LANDSURFACE DEVELOPMENT IN THE MID NORTH OF

SOUTH AUSTRALIA

BY N. F. ALLEY*

Summary

ALLEY, N. F., 1973. Landsurface Development in the Mid North of South Australia. Trans.

R. Soc. S. Aust., 97 (1), 1-17, 28th February, 1973.

The landsurface of the Mid North has resulted from a complex tectonic and erosional history.

During the Cainozoic, faulting formed large basins in which terrestrial and marine sediments were

deposited. The earth movements also initiated two major phases of erosion.

Remnants of a landsurface established in (?) pre-Tertiary times are found high in the relief as

weathered hills and plateaux in places capped by laterite (laterite surface). A probable mid Tertiary

phase of planation is represented by silcrete capped remnants (silcrete surface). It is underlain by

deeply weathered bedrock and occurs only a few tens of metres below the laterite level. The present

broad valley floors, wide intermontane plains and coastal plains (plains and valley surface) had

developed by the Late Quaternary. Etch surfaces are found adjacent to remnants of the two earlier

surfaces.

There is considerable structural control of landforms. Resistant quartzites and sandstones form the

highest parts of the relief, as they also did during previous phases of erosion. Argillaceous strata

have been eroded to form broad valleys, which follow the regional meridional strike. Differential

erosion of these contrasting lithologies, combined with stream piracy, has led to the development of

a trellised drainage system. The River Broughton is the only stream, which has maintained its

westerly, consequent course throughout the Cainozoic, but stream captures have led to large

changes in the drainage patterns of the Light and North Para Rivers.

LANDSURFACE DEVELOPMENT IN THE MID NORTH OF SOUTH AUSTRALIA

by N. F. Avitey*

ALLEY, N. F., 1973. Lundsurface Development in the Mid North of South Australia. Trans.

R. Sov. S. Aust., 97 (1), 1-17, 28th February, 1973.

The landsurface of the Mid North has resulted from a complex teclonic and erosional

histary, During the Cainozoic, faulting formed large basins in which terrestrial and marine

sediments were deposited. The earth movements also initiated {wo major phases of erosion.

Remnants of a Jandsurface established in (?) pre-Tertiary times are found high in the

relief as weathered hills and plateaux in places capped by laterite (Jaterite surface). A

probable mid ‘Tertiary phase of planation is represented by silcrete capped remnants (silcrete

surface). It is underlain by decply weathered bedrock and ocevrs only a few tens of metres

below the laterite level. The present broad valley floors, wide intermontane plains and

coustal plains (plains and valley surface) had developed by the Lute Quaternary, Etch surfaces

are found adjacent to remnants of the two earlier surfaces,

There is considerable structural control of landforms. Resistant quartzites and sandstones

form the highest parts of the relief, as they also did during previous phases of erosion.

Argillaceous ‘strata have been eroded to form broad valleys which follow the regional

meridional strike. Differential erosion of these contrasting lithologies. combined with stream

piracy, has led to the development of a trellised drainage system. The River Broughton is

the only stream which has maintained its westerly, consequent course throughont the Camo

zoic, bul stream captures have led to Jarge changes in the drainage patterns of the Light

and North Para Rivers,

Introduction

The Mid North forms an area of moderate

relicf between the fold ridges of the Flinders

Ranges to the north and the upfaulted plateau

of the Mt. Lofty Ranges to the south (Fig. 1),

The occurrence of fluyio-lacustrine and marine

sediments on ridge tops, along river valleys and

in structural basins indicates that this Tegion

has had a complex history. Remnants of

weathered tesiduals capped by laterite or sil-

crete provide further evidence of this com-

plexity.

It is the purpose of this paper to trace the

sequence of geomorphic events which Jed to

the formation of these features and their

Preservation in the present Jandscape.

Geological Setting

The Adelaide System Rocks

The northern part of the area is underlain by

Willouran, Torrensian and Sturtian strata

(Wilson 1952; Clare 1 : 63, 360 sheet; Forbes

19651). These rocks are arranged in en echelon

folds in the northwest but parallel folds oceur

in the east (Fig. 1), South of Riverton faulting

has resulted’ in the termination and breaching

of the folds (Kapunda 1: 63, 360 sheet; Truro

1:63, 360 sheet). The Kanmantoo Group

occurs here and is underlain by a sequence of

Lower Cambrian sediments (Coats 1960*).

importance af Lithology and Faulting

The major topographic features. reflect the

contrasting rock lithologies. Between Clare

* Terrain Sciences Division. Geological Survey of Canada. Present address, Soils Division, B.C, De-

partment of Agriculture. Kelowna. British Columbla, Canada. Research carried out at the

Universily of Adelaide.

1 Korbes, B. G. (1965).—The ecology of the Clare 1: Mile area. Unpublished report, Geological

Survey of South Australia.

* Coats, R. P. (1960).—The geology of the Kapunda—Truro Military Sheets,.An explanation of the

Geological Maps. Unpublished report, Geological Survey of South Australia.

2 N. F. ALLEY

SOUTH AUSTRALIA

BARUNGA R

ANGE

—_—— ——

\ Narridy

2 Yacka Gorge

3 Spalding Gorge

4 Nantowarra Hills

--7- Approximate

dip and strike of

bedrock

OKm 15

[ere

Fig.

and bedrock structures are shown.

and the Murray Plains, the Gilbert Range

Quartzite underlies the major ridges whereas

dominantly argillaceous strata underlie the

valleys (Fig. 5).

Apart from the quartzite ridges, fault scarps

form the most important physiographic breaks.

The most conspicuous of these is one resulting

a Baloklava

Lr -s-

ty 4 h t

1 ' 4 7

1 ' ' ' ‘

' ! ‘ i r]

' 1 ‘ ' i

! 1 / t 7

' ' 4

4 \ 4 rk 4

1 ' ‘ I

i ' t \ 1

' ' 1 rt

' ' 1 \ ro

i \ 1!

' t 1

\ ‘ a !

1 ' 1S i toy

rope 4 e +; F

4 af | r\o4 tak

U { ert rl \

too) 4 te 1 nS

Ul 1 1 : {oa \ 1 \

x 1 oo p M\er 1 \

a 5 re 2

fon

ey 1 1

‘oa ‘

rm) ‘ 1 i)

o ! 1 ‘

aw}

= F a br

1 ‘ \

& 1 ft

a !

rc) t 1

Undalyay - bs

*Riverton

1. Location, points of reference and general siruciure of the Mid North, Only the major faults

from movements along the Alma Fault west of

Clare, This fault and others divide the Mid

North into a series of north-south trending

blocks (Fig. 1). The youthfulness of many

scarps and the scismicity of the area (Sutton

& White 1968) suggest that the faulting con-

tinues.

LANDSURPACE DEVELOPMENT IN 'THE MID NORTH

Cainozoic Sediments

Although Tertiary marine strata abut the

eastern and western flanks of the ranges, terres-

trial sediments of similar age occur in several

basins and valleys within the uplands (Table

|). Two of the most important of the latter

are the Wakefield and Barossa Basins, Buried

beneath the sediments in these basins is a

partly dissected, weathered and faulted Jand-

surface,

TABLE 1

Terrestrial Sediments of the Mid North

Name

Unnamed

Description and occurrence

Mottled and calcareous red sandy-clays.

Found in major river valleys. intermontané

basins and coastal plains.

Age

(7) Pleistacene

tao Early Recent

Koolwnga Gravels and

siticified sands and

gravels

Rowland Flat Sands

Flavio-lacustrine sands, gravels and boulders

widespread in the Broughton caichment par-

ticularly en the castern margins of the

Wakefield Basin.

Fluvio-lacustrine sands and. gravels found

in the Barossa urea. Lignitic at depth in

the Barossa Valley,

Snowtown Sands

Interbeddéd fluvio-lacustrine

and ligniies found below

Plains.

sands, clays

the Condowte

Clinton Coal

Late Tertiary to

Quaternary

Miucene

Mincene

Middle-Upper

Measures estuarine origin, Confined to the Wakefield Ecocene

Basin,

A. PLUVIO-LACUSTRINE AND MARINE Middle-Upper Eocene beds (Harris pers.

SEDIMENTS comin, 1968). The Miocene strata are

1. WAKEFIELD Basin

The pattern of faults. demonstrate that the

busin ts of tectonic origin (Fig. 1). As it forms

the northern apex of the St. Vincent Basin,

the periodic earth movements and subsequent

sedimentation evidenced in both are necessarily

related,

Deeper Basin Sediments

Bores drilled through the Inkerman-Bala-

kKlava and Whitwarta coal measures penetrated

a considerable thickness of estuarine (Harris

pers, comm. 1968), marine and lacustrine de-

posits. (Johnson 1959; Hillwood 1960). The

sequences of the Balaklava area are complex

and interpretation of the deposits. in particular

the estuarine lignites, is uncertain, However,

recent studies refer the latter to the Middle-

Upper Eocene (the Clinton Coal Measures of

Hartis 1966), und the overlying marine beds

to the Oligo-Miacene (Hillwood 1960). ‘The

northern and eastern limits of the marine beds

lic along the Bowmans and Mt. ‘Templeton

Fuults. At Snowtown the marine deposits are

absent but interbedded carbonaceous clays,

sills und sands of Miocene age overlie the

lacustrine and terminate in the south along the

Balaklava Fault, Because of their stratigraphic

relationship to the Early Tertiary beds and

their dominantly sandy lithology, the Miocene

strata are separaled from the former and here

named the Snawrown Sands, The type section

is from stratigraphic borehole 4A on the

northern edge of Snowtown and the strati-

graphic relationships are shown in Figure 6.

‘The mid Tertiary marine sequences and the

Snowtuwn Sands are separated from each other

by «a horst, known as the Nantawatra Hills,

which resulted from uplift along the Bowmans

and Balaklava Faults {Fig. 1). The absence

of the Oligo-Miocene sediments from the sur-

face of the horst and their occurrence at the

foot of the bounding fault scarps on the north

and south suggests that the faulting predates

the Middle Tertiary.

Marginal Sediments

Numerous deposits of highly siliceous sands

and gravels occur along the fringes of the

Wakefield Basin. Small outcrops abut the

eastern front of the Barunga Range but Jarger

deposits occur in the valley of the River

Broughton on ihe eastern edgé of the basin.

N. FL ALLEY

4 Gulnare

Fluvios (ucustrine deposits. _-

Surface exposures of the ~ 4)

Koolunga Gravels :

Uplands,

OKm 5

——

‘Alma Fault

2. The distribution of the Koolunga Gravels in the middle and upper Broughton drainage basin.

The dips. of the faults in the Mt, Gregory Range are unknown,

The most prominen| crop out near Koolinga.

Yacka and Spalding (Fig, 2). These deposits

are here named the Koolungu Gravels and the

lype section is located at White Cliffs, 4 km

east of Koolunga in the south bank of the

Broughton River (Fig. 10).

The western edge of the Koulunga Gravels

is marked by a low rise which may represent

the northern extension of the Owen Fault

Scarp, for bore logs indicate that they continue

al depth further westwards. At White Cliffs

the gravels overlie an. itregular surface eroded

across Precambrian bedrock (Fig. 10). Move-

ment along a fault zone in the latter has led

toa J m dislocation of the overlying deposits.

The best exposure of the beds occurs in the

Yucka Valley where deltaic sands and gravels

containing boulders of silcrete overlie gently

dipping Precambrian sandstone. These deposits

can be traced across the ridge marking the

western flank of the valley, but the Alma Fault

scarp separates them from the Koolunga

sequences (Fig, 2). Because of their similar

pebble lithologies, in particular the presence

of silerete in both, the Yacka and Koolunga

beds were probably deposited contempor-

angously and have since been displaced by

faulting with the downthrow to the west.

Whether the highly siliceous gravels south

and cust of Spalding were deposited in the

same lake is a matter for conjecture, for they

stand 100 m higher than those at Yacka (Fig

2). The difference in height between the two

deposits may reflect a fallmg lake level or fault-

ing, or the Spalding gravels may not be corre-

lative with the Yacka heds and instead be en-

tirely fluviatile, However, the presence of

xilerele houlders in the Spalding gravels indi-

cutes that they may have been deposited con-

temporaneously with the Koolunga Gravels.

Although no fossils were recovered from the

Koolunga Gravels, there 1s evidence to suggest

that they post-date the mid Tertiary, At White

Cliffs and Yacka the gravels contain boulders

of silcrete. a rock assigned lo a probable Middle

IT ANDSURFACE DEVELOPMENT IN THE MID NORTH 5

Tertiary weathering phase (see below). North

and west of Yacka, outcrops of the gravels

overlie an etch surface related to the erosion

nf the silcrete surface (Fig, 3). Thus, the

Koolunga Gravels do not represent a shoreline

facies of the Snowtown Sands but were de-

posited at different times in a Jake occupying

the same basin.

Silerete &

~koolunga

Gravels

(exhumed }

Fig. 3. The stratigraphic relationship between

the Koolunga Gravels und the silcrete

surface in the Yacka area, Only the sur-

face exposures of the gravels are shown.

2, Bakossa Basin

These include the fluvio-lacustrine sediments

deposited east of the Para Fault in the Barossa

and Stockport-Freeling areas (Pig. 4).

The strugture of the Barossa Valley is not

completely Known. Tt has been described as a

graben (Hossfeld 1949), a Fault angle valley

(Chuge 1955), and an asymmetrical synctine

with q fault or flexure along the southeastern

flank (Dalgarno 19613; Olliver 1962). Never-

theless, the nature of the Tertiary strata ¢on-

tained by the valley is well documented (for a

review of this work see Dalgamno 1961, and

Harris & Olver 1965). West of Rowland Flat

a basal deltaic unit is overlain by a sequence

of sands and gravels characterized by medium

und Jarge scale deltaic bedding (the Rowland

Flat Sands Conglomeratic Lens and the Row-

hind Flat Sands of Dalgarno 1961), whereas

lignitie sands have been encountered at a

depth of 30 ta 100 m during boring in the

Rowland Flat-Tanunda plain (Chugg 1955),

As there is no stratigraphic evidence for

scpurating the conglomeratic lens from the

overlying sands, it is proposed that it be in-

cluded as part of the Rowland Flat Sunds.

Scattered outcrops of the sands extend west-

wards across the Kitchener Fault to the Gawler

area, and northwards to Stockport (Fig. 4).

They were probably deposited contem-

porancously with the Rowland Flat Sands as

the beds occur within the same range of eleva-

tion (Fig. 4). Moreover, the Lyndoch-Sandy

Creek deposits ure characterized by the same

mineral assemblage as those at Rowland Flat

and are thus regarded as the westerly extension

of the Barossa sequences (Olliver & Weir

1967).

Although the Rawland Flat Sands. have been

assigned a variety of ages, recent palynological

evidence indicates « Miocene age, making them

time correlative with the deposits northeast

of Gawler (Haris pers. comm. 1969).

B. ALLUVIAL DEPOSITS

Red alluvium covers most of the low-lying

iireas, varying from a Tew metres in minor

creeks to 36 m in depth at Balaklava. In the

Barossa Valley and near Red Ranks, bores

show that the sandy clays exceed 30 m in

thickness. Although the alluvium is 15 m deep

in the Yackamoorundie Valley downstream

from Georgetown, it rarely exceeds 6 mm in the

upper reaches of other main Valleys, In most

areas the alluvium is mottled and calcareous,

Suggesting some measure of weathering since

its deposition.

The alluvial clays are interpreted as a

Pleistocene deposit in the Port Wakeficld area

(Johnson 1959; Hillwood 19640; Horwitz 1961)

7 Dalgarno, C: R. (1961}—Geology of the Barossa Valley. Unpublished M.Sc. Thesis. Universily of

Adelaide.

6 N. F. ALLEY

Sandy Creek

"215 Spot Height imetres! Q cnt

266

Para Fault

Fig.

and the Burossa Walley (Campana 1955;

Chugg 1955). On the basis of radiocarbon dat-

ing, the red clays. north of Adelaide have been

assigned to the Late Pleistocene (Williams

1969}, Mottled clays (the Hindmarsh Clay of

Firman, pers. camm, 1968), overlying a Plio-

cene marine bed at Red Banks are believed to

be of Pleistocene age.

On this basis the heavily calcified red clays

in the Mid North have been placed tentatively

fee

5 lyndoch, SS

sKAPUNDA

-—— Moin uplands

=| Rewland Flat

: Sands (sic. exo.)

4. The distribution of the Rowland Flat Sands in the Barossa-Freeling area. The differences in

height of the deposits in the latitude of Freeling may be related to post Miocene earth move-

ments,

in the Pleistocene to Early Recent though they

may vary in their precise age or age-range from

locality to localily.

C, WEATHERED LAND SURFACES

BURIED BENEATH THE CAINOZOIC

SEDIMENTS

In the Snowtown area only a few bores

penetrate to the Precambrian but these reveal

that the basin floor is irregular and weathered.

LANDSURFACE DEVELOPMENT IN THE MID NORTH 7

At a depth of 69 m, stratigraphic bore No. 4A

located at Snowtown, penetrated 27 m of

highly weathered sandstone, Three kilometres

north of Snowtown unweathered bedrock

occurs at 49 m, but Icss than 1.5 ko east of

this location the basin floor deepens to 111 m..

{ f

OMintate f

‘The weathering of the basement rocks probably

predates. the deposition of the overlying Ter-

tiary sequences for bore logs indicate that the

latter are essentially unweathered,

The nature of the buried surface beneath the

Rowland Flat Sands is better known. Bore logs

Q Merildin

S lerete leyrmeants

¥e8 +566 Spot height (r

OWotervale

a Gilbert Ronge Quartzite

Weathered residual) and etch

plains related to the

laterite level

=— Loierite level

Fig. 5. Remnants of the laterite and silcrete surfaces near Merildin. The Gilbert Range Quarizite

underlies the major ridges, while dominantly argilliceous strata crop out in the valleys.”

+ WN, F. ALLEY

indicate that the basement rocks are weathered

in the Barossa Valley (Chuge 1955). At Row-

land Flat the unconformity surface has a local

telief of up ta 15 m (Olliver & Weir 1967)

and the Rowland Flat Sands overlie both fresh

and weathered bedrock (Fig. Ll). At ©. R,

Hueppau!’s quarry, on the north bank of the

North Para River, Torrensian bedrock is

weathered and highly ferruginized. Between

Sandy Creek and Warpoo Siding, highly

kuolinized mica schist underlies the sands.

South and west of Frecling the sands were de-

posited on subhorizontal bedrock surfaces,

though only small remnants of the Tertiary

sequences remain. Thus it appears that the

Rowland Flat Sands were deposited on a partly

dissecied erosion surface underlain by highly

weathered and ferruginized bedrock.

Surfaces uf Degradation and Deposition

Investigations reveal that remnants of three

major surfaces of erasion and deposition occur

in the Mid North. The highest and oldest of

these is capped discontinuously with laterite.

Below this is another erosional surface which

supports a thick crust of silcrete, The youngest

surface ls largely depositional and the alluvial

clays underling it ure heavily calcified, Etch

plains of considerable extent developed as a

result of the dissection of the laterite and sil-

crete surfaces,

Larertte Surface

Apart from the prominent ridges underlain

by quartzite and sandstone, remnants of the

laterite surface form the highest parts of the

lajdscape. Where, the laterite truncates thick

Precambrian argillaccous strata, slopes vary

belween 1° and 2° (Fig, 12), However, near

the quartzite ridges remnants of pediments

exhibiting slopes of up to 7° are found, Such

residuals are common in the ranges euse of

Clare (Fig. 5) and Riverton, Remnants of the

laterite surface are more numerous at the

streum) Heads. Nevertheless, by virtue of their

resistant capping they alsa fonm prominent. hills

standing nearly 100 m above valley floors.

yome distance from the ridges (Fig. 13).

The laterite capping, which consists essen-

tially of angular quartz set in a matrix of tron

oxides, is underlain by heavily weathered and

locally kaolinitic bedrock (Fig. 14>. Only the

massive quartzites and sandstones remain uny-

altered and these stand 30-180 m ubove the

general surface level) A zone of intense

weathering often lies at Ihe head of the pedi-

{nent Férnnants Which slope away from these

scarps wheras the Jaterite crust is consistently

thickest on the lower slopes.

The etching away of the weathered strata

from beneath the laterite has let to the

exposure of broad bedrock surfaces, It is

usually the case that these etch surfaces lie

15-30 m below the laterite surface and

separated from it by seep scarps. Because of

strong lithological control during weathering

and subsequent erosion, the etch surfaces are

often irregular with argillaceous strata forming

the vallevs, and sandstones the ridges (Fiz.

13),

Silerete Surface

Evidence of a former erosion surface capped

by silcrete and consistently lower than the

height of the faterite is found throughout the

Mid North (Fig. 15). It reaches its optimum

development around the northeastern fringe

of the Wakefield Basin (Fig, 6), Here slopes

can be less than 1°” whereas slopes as great

a8 4° have heen encountered elsewhere. Like

the laterite, the silerete surface truncates rocks

of ull types, except the thick quartzites, and

1s Underdain by some 15 m of intensely ksolin-

ized bedrock. North of Narridy the weathering

reaches a depth of 30 m, bul this is probably

duc to the porosity of the underlying sandstonc.

Fertuginuus hurtzuns are common in the

weathered zone developed across argillaccous

strata (Fig, 7),

‘The nature of the silerete crust is variable

(Figs. 7, 16). Higher parts of the surface are

weakly silicified or suppart a thin capping of

consolidated regolith. Silcrete lower in the

relief is generally thicker und finer grained, In

many areas where the silcrete has heen broken

up. a thick lag of boulders remains as a pro-

tective veneer over the weathered bedrock,

An extensive etch plain developed following

dissection of the silerete surface, particularly

where the main streams cut deep gorges

through the silercte level. Thus prominent bed-

rock benches occur slong the Rocky Rivet

downstream from Gladstone and the Yacka-

moorundie Creek west of Gulnare. This sur-

face is often capped by a silicificd congtom-

erle containing Lragments of silcrete derived

from adjacent silcrete remnants (Fig, 17),

Because the conglomerate has all the charac-

|_ANDSURFACE DEVELOPMENT IN THE MID: NORTH 9

oBurra _ 4

Murray

Laterite Bid:

ans

remndnts

dominate

Largely silcrete remnants

Areas farming

probable Miocene lake basins

s Gkm

| ce |

= cr 2 f

as DGawler-—-E= ——

ras Leterjte

Nantawarro Hills

A a i Silcrete S

a Lote Quaternary alluvium

~*< = =a = ee

S 3 2

\ = Weathered Pre £

~ ri ~~, “

Balaklava Fault

Fig, 6, The distribution of laterite and silcrete remnants in the Mid North, and the stratigraphic re-

lationship between the surfaces bordering the Wakefield Basin. The diagrammatic section

(not to scale) has been constructed from bare logs. From the surface, 1$ m of plains and valley

alluvium are underlain by 15 m of silts and clays, 23 m of Miocene Snowtown Sands and 35

m of Middle-Upper Eocene Clinton Coal Measures (E). Both the latter units vary consider-

ably in thickness, The Mt, Templeton Fault occurs in the breached part of the section.

(a N. F_ ALLEY

Raolinized

“

sondstone

‘gin oF, tren oxides

a | fr

3. West of Kupunde

Fig, 7. Variations in the silcrete crust and its

underlying weathering profile in the Mid

North,

Section 1: Zone A consists of pisolitic

silcrete; B laminar sitcrete; C is a com:

plex zone grading downwards from sili-

cified sandstone to very resistant por-

celanitic silcrete.

Section 2: Zone A, massive crypto-

crystalline silerete; B, weakly silicified

sandstone; C, very weathered rock con-

tuining abundant angular fragments of

quartz.

Section 3: Zone A, massive crypto-

crysialline silercte containing numcrous

rounded quartz pebbles near its base.

teristics of a sedimentary rock and uncon-

formably overlies fresh Precambrian at

numerous sites, it is not interpreted as a second

period of silcrete formation and is referred to

as silicified sands and gravels. On the basis of

its relationship to the etch surface these sedi-

menis were probably deposited in valley

bottoms contemporancously with the Koolunga

Gravels.

Relative Ages of the Laterite and Silcrete

The laterite surface forms the flat upland of

the Nantawarra Hills (Fig. 6), To the ease

and north of the hills, the surface has been

downfaulted and the Middle Tertiary sedi-

ments occur at the base of the fault scarps

suggesting that the laterite surface in this areca

may be Early Tertiary or older, In this case,

the surface buried beneath the Middlc-Wpper

Eocene lignites in the Snowtown region could

be the equivalent of the laterite surface, On

the other hand, if the lateritized surface un-

derlying the Rowland Plat Sands is correlative

with the laterite surface, the Jatter must have

persisted in the Barossa area until the mid

Tertiary when earth movements led to its dis-

section and partial burial.

ii is difficult to assign an age range to the

silerete surface, although mapping reveals that

it is consistently Jower than the laterite surface

even where they truncate the same strata (Fig.

8), Thus the difference in their heights is due

to crosion rather than Jithology, and it can be

inferred that the silerete is younger than the

laterite surface. However, the optimum de-

velopment of the silcrete surface occurs around

the fringes of the Wakefield Busin, There is

evidence lo suggest that the early ‘Tertiary

Fig. 8. The altitudinal relationship between the

laterite and silcrete: surfaces west of

Georgetown. The bedrock strike is

approximately north-south, ard both

surfaces are eroded across the same

strata,

LANDSURFACE DEVELOPMENT IN THE MID NORTH It

esluatine swamps and then the Miocene lake

which occupied this basin may have formed

the base level af erosion for the silcrete sur-

face in the surroundiig area, First, the surface

slopes vently towards the basin. Second, the

Eocene estuarine and the Miocene Jacustrine

sequences are generally fine, suggesting that

deposition Was cantemporaneous with the ero-

sion of a plain of low relief which is consistent

with the gentle slopes observed on the silcrete

remnants, Third. no silcrete is recorded from

the borcholes drilled through the Tertiary

secliments,

Present Valley Floors and Plains

The must extensive surface of ageradation in

the study area is the Condowie Plain (Fig.

1), Near Snowtown the plain measures almost

4 km from east to west, whereas in the

noflbern part near Redhill the basin is Jess

than § km wide. The Condowie Pliin con-

tinkes southwards and gradually merges with

the Adelaide coastal plains south of Baluklava.

In the latitude of Snowtown the surface of the

plain is gently undulating but asymmetrical

wilh a long. fall from the Alma Fault scarp

on the east. No streams traverse the plains

excep! along the northern fringes: Where the

Broughton and its two lurge tributaries, Rocky

River and Yackamoorundie Creek, are incised

up to 9 m in the red alluvium.

Two other intermontane basing oceur: the

Barossa Valley and athe Yackamoorundie

Valley south of Georgetown, the later con-

twining an alluvial fill 54 m in depth. The

surfice of the Barossa is similar to the Con

dowie Plain. displaying east-west asymmetry.

Broad alluvial Fans front the Barossa Ranges

near Rowland Plat, gradually giving way to a

gently sloping surface further north. Along the

westerh edge of the basin the plain extends

across aulcrops of the Rowland Flat Sands as

a lightly ferruginized erosional surface.

Age of the Plains and Valley Supfice

Vhroughout the Mid Novth, the red cal-

carcous clays are the most common deposits

underlying the surface. This alluvium has been

assigned a Pleistocene to Recent age (see

above), and thus the surface must be approxi-

mately the sume age, In the Barossa where it

(runciles the Middle ‘Tertiary lake sediments,

portion of the surface may belong to the Late

‘Terriary

Development of the Drainage System

The Mid North is drained by two sets of

river systems: the Broughton, flowing to Spén-

cer Gulf, and the Wakefield, Light ani North

Para Rivers. to St. Vincent Gulf, The history

of change in this drainage pattern can be

determined by an examination of the nature of

the Tertiary sediments and landsurfaces.

A. INFLUENCE OF LITHOLOGY AND

STRUCTURE

The perfection of lithologies) adaptation of

the drainage is a feature of the area. In broad

view lithology determined the direction of

drainage on the two duricrusted surfaces, Once

the weathered mantle was removed from these

surfaces. intricate irregularities in lithology

controlled the course of erosion. Consequently,

the present drainage exhibits 4 trellised pat-

tern, the long subsequent (strike) streams

flowing in valleys underlain by argillites while

the resistant sandstones and quastzites remain

as the fidges. The north-south trending prat-

fern of the major streams results from = the

meridional strike of the fold axes (Fig. 11.

B. CHANGES IN THE PATTERN DURING

THE CAINGZOIC

The long meridional trending reaches of the

strcams have heen interpreted as the dismem-

bered drainage of a Tertiary peneplain (How-

chin 1933; Hossfeld 1935; Langford-Smith

1949), Such a postulate may only be applied

to the St. Vincent Guif drainage.

1. Tie River BroucHTon

Based on the evidence of elbows of capture,

abandoned valleys containing riverine graveis

and increased gradients in the gorge sectors of

the newly formed valleys, Langford-Smith

(1949) demonstrated that stream piracy

occurved amongst minor tributaries in the

Jumestown area. In view ol the elbows and

gorges slong the Broughton, he applied the

theory to the whole drainage basi, He pro-

posxd that the river captured a system of

southerly flowing streams from ihe west sub-

sequent upon uplift of a Tertiary Jundsurface.

Faulting aided local ponding of the stream

and hastened the speed of capture.

However, investigations cannot substantiate

the theory. Only two gorges occu’ along the

Broughton, ohne west of Yacka and the other

west of Spalding, No knickpoini is found in the

Yacka reach while those in the Spalding gorge

fesulk [rom lithology or structure. There is no

2 N, F. ALLEY

evidence of a former south flowing stream

system, the development of which was pro-

hibited by the geologic structure of the arca

and the resistance of the Gilbert Range Quart-

zite, Upstream from Yacka the drainage pat-

tem may have been in existence since Early

Tertiary times, for remnants of the laterite

surface slope towards major streams whereas

their heights decrease down-valley in the direc-

tion of present drainage. Many of the Caino-

zoic gravels, some of them lacustrine, occur

both on intervening ridges and in several

gorges, instead of only in the broad strike

valleys, As uplift of the Tertiary landsurface

occurred along N-S trending faults, there

should have been no local impounding of south

flowing rivers. Moreover, the disposition of the

Cainozoic sequences in the Yacka-Spalding

area suggests faulting after depositton, not be-

fore. Finally, if stream piracy has occurred, it

is the Broughton system which is being cap-

tured not the reverse (Fig. 9}.

The middle and upper reaches of the

Broughton have remained essentially unmodi-

fied and it is only downstream from Yacka

*Menldin

. Stream capture of the upper Farrell

Creek near Merildin. The nature of the

barbed drainage within the enclosed sec-

iron and the pronounced elbow of the

Wakefield downstream from Merildin

indicates. that the pirate stream was the

River Wakefield.

that the evidence suports changes in the put-

tern.

Focene. lignites extend at depth to within

a few kilometres of Koolunga where the

Broughton turns north-westwards to flow

across the northern perimeter of the Condowie

Plain. If the upper reaches have altered little

since the Early Tertiary, it is logical that the

river made its way to the present St, Vincent

Gulf area through the tectonic yalley which

came into existence at this time (sce aboye),

lt is probable that uplift of the Nantawarra

horst in the mid Tertiary blucked the valley,

leading to the formation of a lake, A larger

lake resulting from reactivation of upwarping

in the Late Tertiary or Quaternary either over-

flowed the Baruhga Range or was captured

from the west (or both) and the Broughton

fiowed into Spencer Gulf.

2. St, VINCENT GULF DRAINAGE

A striking feature of the drainage pattern

of these rivers. is the absence of major south

bank tributaries (Fig. 1), An eaamination of

the Cainozoic sediments and the Tertiary land-

surfaces reveals that only stream piracy can

account for the anomaly.

The long quartzite ridge east of Tarlee was

a major drainage divide in Early Tertiary

times. All laterite remnants slope away frem it

as far north as Manoora and south as Green-

ock, Erosion of this surface by separate drain-

uge systems is indicated by large diiferences

in the height of residuals on opposite flanks

of lhe ridge. The river east of the ridge occu-

pied the valley of the upper River Light und

flowed southwards along the present Barossa

Valley area whereas the other approximutely

paralleled the course of the Gilbert River.

However, there ts no evidence to suggest that

the River Wakefield had yet been established.

Consequent upon the mid Tertiary earth

movements were the dissection of the laterite

surface and the formation of a Jake in which

the Rowland Flat Sands were deposited. The

two south flowing streams probably enterudd

the lake at the northern edge of the Barossa

Valley and near Stockport. This is borne owt in

these areas by the coarseness of the gravels,

the palacocurrents and the mineral assemblage

(Dalgarno 1961, Alley 19694).

In Late Cainozoic times the majar stream

east of the divide was captured from the west

LANDSURFACE DEVELOPMENT IN THE MID NORTH 13

by two separate streams, one forming the

present lower reaches of the River Light now

confluent with the Gilbert River, and the

other, the North Para River. Stream piracy is

supported by several lines of evidence, First,

prominent elbows occur on the rivers where

they turn westwards to flow across the strike

of the bedrock (Fig. 1). Second, an abandoned

valley due south of Rowland Fiat and infilled

with Tertiary sediments may represent the

former channel of the beheaded stream. Third,

hoth portions of the newly formed streams

have cut deep charinels into the Rowland Flat

Sands, suggesting that the excavation post-dates

the mid Tertiary,

Although a prominent elbow occurs en the

River Wakefield at Undalya, where the river

turns into a gorge and flows across the strike

nothing other than the lack of major south

bank tributaries to suggest that capture may

have taken place,

Landscape History

Remnants of three major Jandsurfaces have

been described and discussed (Table 2). Since

the dissection of the Jaterite surface, differen-

tial erosion has led to increasing relief. Where

the ridges formerly stood 90 to 180 m above

the level of the laterite surface, they now pro~

ject more than 300 m above valley floors.

Early Tertiary earth movements in and

around the Wakefield Basin probably led to

the disruption of the laterite surface in the

Broughton drainage system and the establish-

ment of a new phase of erosion during which

of extremely resistant

TABLE 2

Surfaces in the Mid North

quartzites, there ts the silcrete surface developed. Broad etch sur-

Surface

Plains and valley

Description and origin

Major valley floors, intermontane basins

and coastal plains, Narrow. erosional pied-

mont zone fringing these areas, Mainly

aggradational.

Unweathered bedrock surfaces ‘standing

below and adjacent to the silcrete surface

in the Broughton catchment. Developed

subsequent te removal of weathered zene

beneath the silérete, Buried by lacusitine

gravels in some localities bul exhumed jn

others,

Probable age

Late Tertiary (7?) to

Early Recent

Initiated in the Late

Cainzaic

Silcrete

Silicified mesas and valley sides occurring

throughout the Broughton catchment. fso-

lated remnants near Kapunda, Freeling and

Owen. Resulted from erosion and weather-

ing.

High unweathered bedrock benches devel-

oped below and adjacent to the laterife sur-

face as a result of removal of the weathered

mantle from below the laterite.

Laterite

Broad plateaux and mesas capped by later-

ite and, apart from quartzite ridges, form-

ing the highest parts of the relief. Resulted

from erosion and weathering.

Mid Tertiary

Initiated in the Early

Tertiary

{7) Early to pre

Tertiary. Persisted to

mid Tertiary in the

Barossa area.

faces resulted from the removal of the deeply

weathered muntle much of which was de-

posited lower in the relief as. the Middle-Upper

Eocene sediments, and later in the Miocene

as the Snowtown Sands. The laterite surface

persisted in the Barossa area until the mid

Tertiary when renewal of the faulting led to

its dissection, The earth movements probably

dammed streams, leading to the formation of

a basin in which the Rowland Flat Sands ac-

4 Alley, N. F. (1969).—The Cainozoic history af the Mid North of South Australia. Unpublished

M.A. Thesis, University of Adelaide.

14 N

cumulated, As these sands and the Snowtown

Sands are contemporaneous but deposited in

separate tectonic basins, it is logical to argue

that the earth movements were widespread

during the mid Tertiary,

There is evidence to suggest that the fault-

ing continued, In the narth, earth movements

account for the dissection of the silcrete sur

face, the development of broad etch plains and

the deposition of the Koolunga Gravels con-

temporancously with the silicified sands and

gravels. Recent earth movements were respon-

sible for the dislacation of the Koolunga

Gravels at White Cliffs and in the vicinity of

Yacka. Deposition of the plains and valley

alluvium and the alluviul fans abutting the

Alma and Kulpara Fault scarps may also have

heen initiated during this period.

If the buried surfaces beneath the Tertiary

sediments in ihe Wakefield Basin and the

RB ALLEY

Barossa Valley are analagous to the Jaterite

surface, it has suffered faulting or warping in

the order of 300 and 180 m respectively in

these areas.

Acknowledgements

The thanks of the writer are due to: the

South Australian Department of Mines for

making bore Jog data and unpublished reports

available; Mr. W. K. Harris, 8, Aust. Depart-

ment of Mines, for his advice on the Tertiary

stratigraphy; Mr. A. R. Milnes, Department of

Geology, University of Adelaide, for his

guidance in the analysis of the duricrust pro-

files; Mr. M. J, C. Walker, University of Edin-

burgh, for his critical reading of the text; and

Dr, C. R. Twidale, Department of Geography,

University of Adelaide, for his valuable com-

ments in the ficld and on this paper.

References

Camerana, B. (1955) —Lhe geology of the Gawler

Military Sheet. Rep. Invest. geal Surv. §.

Ast, 4, 1-22.

Cuucs, R. — (1955)—The hydrology of the

Rarossy Valley, Refi. Invest. geol. Surv. 8.

Aust, 2, 1-77,

Coats, R. P. (1959)—Trure map sheet, Geolo-

gical Ailaus. of South Anstralia, 1763, 360

series, (Geol, Surv. 8, Aust.: Adelaide.)

Dickmson, 8. B. & Coats, R. PB. (1957)—

Kapunda map sheet, Geological Atlas of

South Australia, 1:63, 360 scrics. (Geal.

Surv. S. Aust.: Adelaide.)

Fortis, B. G. (1964)-—Clare imap sheet, Geo-

logical Atlas of South Australia, 1:63, 360

series. (Geol, Surv, S, Aust: Adelatde.)

Harris, W. K. (1966) —New and redefined names

in South Australian Lower Tertiury strut

graphy. Quart. geol. Notes, geol, Sun §

aust. No. 20.

Harais, W. K. & Ouniver, J. G. (1965),--The

age of the Tertiary sands at Rowland Fiat,

Burossa Valley, Quart, geal. Notes, geal.

Sarv. 8, Aust. Na. $3,

Hitt woop, E. R. (1960)—Inkerman-Balaklava

coalfield, Min, Rev. Adelaide 112, 26-46,

Hoawitz, R. C. (1961).—The geology of the

Wakefield Military Sheet. Rep. Invest. geal.

Sary. §, Aust. 1B, 1-32,

Hosseeep, P. S. (1935)—The geology of part

of the north Mt. Tafly Ranges, Tras. R. Soc.

S. Aust. 59, 16-67.

Fie 1, At White Cliffs, 4 km cast af Koolunga, Late Cainozoic (7) Muvio-lacustrine sands and gravels

containing boulders of silerete have been folded: The monoclinal fold (M) indicates that 4 to

5 m of displacement has occurred. The folding is of the posthumous type and hax resulted

from movernents in the underlying contorted Precambrian phyllitic shalcs which upper in

the lower left (P)-.

Fig. |!, The irregular unconformity surface between the subhorizontally bedded, Miocene Rowland

Flat Sands. and steeply dipping Precambrian schists in a quarry west of Rowland Flu,

Fig, 12, A few kilometres west of Georgetown temnants of the laterite surface occur, Here the surface

slopes gently away from an unweathered core of Precambrian rocks known us Mt. Herbert

(right), The laterite crust is underlain by 2 to 25 m of kaolinized shales some of which

can be seen forming the white areas on the flanks of the two residuals,

Fig.

13. ML Allen. a lateritic, weathered residual eroded across green silty shales in the snout of a

syjicline & km due north of Kapunda. The arcuate, low ridge covered by gums and almost sur-

rounding Mt. Allen consists of unweathered Marinoan quartzite (A,B.C.7}. Differential ere-

sion of adjacent weathered strata, has. accentuated the prominence of the ridge and resulted in

an irtegolar etch surtace.

MID NORTH

IN THE

| ANDSURFACE DEVELOPMENT

——

— | =

ALLEY

N. F.

NAYS

LANDSURFACE DEVELOPMENT IN THE MID NORTH 7

HossFELb, P, S. (1949).—The significance of the

occurrence of fossil fruits in the Barossa

sekungsfeld, Trans. R. Soc. S. Aust, 72, 252-

258,

Howcuin, W. (1933).—The dead rivers of South

Australia, Part IT. The eastern group, Trans.

R. Soc, S. Aust, 37, 1-41.

JauNson, W. (1959).—Coal exploration, northern

end of the St. Vincent Basin. Adin, Rev-

Adelaide 110, 134-144.

Jounson, W. (1964).—8urra map sheet,’ Geo-

logical Atlas of South Australia. 1763, 360

series. (Geol. Surv. S$. Aust.: Adelaide.)

Lancrorp-SmMitH, TT. (1949),—The geomor-

phology of the County Victoria. South Aus-

tralia. Trans. R. Soc, S. Aust, 72, 259-275.

Outiver, J. G. (1962).—Test boring—Rowland

Flat Sand deposit. Min. Rev. Adelaide 121,

144-150.

Ox.iver, J. G. & Wrir, L. J. (1967).—The con-

Struction sand industry in the Adelaide met-

ropolitan area, Rep, Invest. geol. Surv. 8.

Aust. 30. 1-106.

Sutton, D, J, & Wnite, R. E. (1968).—The

seismicity of South Australia, J. geol, Soc.

Aust. 18, 25-32.

WiritaMs, G, E. (1969).—Glacial age of pied-

mont alluvial deposits in the Adelaide area,

Sauth Anstralia. Aust. J. Sei, 32, 257.

Witson, A. F. (1952)—The Adelaide System as

developed in the Riverton-Clare region.

northern Mt. Lofty Ranges, South Australia.

Trans. R. Soc, S. Aust, 75, 131-149.

Fig. 14. Highly weathered Sturtian slates and gritty shales exposed beneath the laterite surface in

Bartsch’s quarry west of Kapunda. The rock is locally kaolinitic, the Iatler being closely re-

lated to bedding planes and joints. Hcight of the section is ahout 15 m.

Fig. 15. Silcrete capping the crest of an erosional scarp several kilometres north of Narridy. In places

the underlying porous sandstone is weathered &) 4 depth of 30 m or more (Fig, 7. Section 1).

An etch surface occurs to the left and lower than the silerete,

Fig, 16. Pisolitic silerete capping portion of the scarp north of Narridy (see Fig. 15). The larger con-

cretions consist entirely of slightly ferruginous silerete, but smaller nodules contain porcelan-

ous kaolin, small rounded grains of silica and a few minor pockets of iron oxides. The piso-

liths are set in a matrix of slightly silicified sandstone. Pen provides scale.

Fig. 17,

Boulders of the silicified sands and gravels (right) scattered over an etch surface developed

adjacent to the silerete surface Cleft), in the valley of the Rocky River several kilometres

south of Gladstone, The gravels unconlormably overlie steeply dipping unweathered Torren-

sian slates and shales.

AUSTRALIAN ACANTHOCEPHALA, NO. 14. ON TWO SPECIES OF

PARARHADINORHYNCHUS, ONE NEW

BY S. J. EDMONDS*

Summary

EDMONDS, S. J., 1973. Australian Acanthocephala, No. 14. On Two Species of

Pararhadinorhynchus, one new. Trans. R. Soc. S. Aust. 97 (1), 19-21, 28th February. 1973.

A new species of Acanthocephala, Pararhadinorhynchus coorongensis, is described from the fish

Aldrichetta forsteri (Cuvier & Valenciennes) from South Australia.

AUSTRALIAN ACANTHOCEPHALA, No, 14. ON TWO SPECIES OF

PARARHADINORHYNCHUS, ONE NEW

by S. J, EoMonps*

Summaty

Epmonps, §. J.. 1973. Australian Acanthocephala, No. 14. On Two Species of Pararhadineor-

Avachus, one new. Trans. R, Soc. §. Aust. 97 (1), 19-24, 28th February, 1973.

A new species of Acanthocephala, Pardrhadinorhynchus coorongensis, is described from

the fish Aldrichetta forsteri (Cuvier & Valenciennes) from South Australia.

Introduction

Johnston & Edmonds (1947) erected a new

venus Pararhadinorhynchus based on P.. mugi-

fis, a parasite from Mugil cephalus Linnaeus.

On several occasions during the last ten years,

a second species of the same genus has been

found in South Australia in the mullet Aldri-

chetta (=Agonestomus) forsteri (Cuvier &

Valenciennes), The new species is described

here and the re-checked dimensions of the

introvert and egg of P. mugilis are given. How

Specific the two parasites are in their distribu-

tion is not clear because collectors have some-

limes confused the two hosts. The identifica-

tions of the fishes carrying the parasites are

based on the descriptions given by Scott

(1942).

Pararhadinorhynchys coorongensis n.sp,

FIGS. 1-5

Host: Aldrichetia forsreri (Cuvier & Valen-

ciennes).

Localities; (1) Coorong, S.A.: coll. J. Harris,

1962. (2) Port Willunga, S.A.; coll. T. H.

Johnston, 1927: (H.C, 1055). (3) Fish

from Adelaide Fish Market (class material.

coll. &. J, Edmonds, 1969, 1971). (4) Pish

from Adelaide Fish Market: coll. H. Man-

ter, 1967,

Type specimens (male and female): Aus-

tralian Museum, Sydney.

Description: Size moderate; shape cylindrical

to sub-spindle-like, slightly broader in anterior

third or quarter. Posterior region may taper

slightly, Posterior extremity sometimes

rounded or slightly swollen,

Trunk of female 9-15 mm long x 0.45-

0.55 mm. Trunk of male 7-11 mm x 0,40—

0.70 mm. Trunk without spines.

Introvert. cylindrical to club-shaped; the part

bearing hooks 0.51—0.62 mm long in female

and 0,50-0.58 mm in male. Maximum width

0.15-0.22 mm in female and 0,12-0.23 mm in

male, Fourteen to sixteen, usually 16, longi-

tudinal rows of 8-10, usually 9, hooks per

row (Fig. 2). Short unarmed neck (0.15 mm

long) in some specimens. Introvert sheath

double walled, 0,6-0.8 mm long x 0.18-0.26

mm wide. Lemnisci about twice as long as

sheath and usually slightly swollen posteriorly,

Position of brain not known,

Female complex relatively long, 2,8-3.4

mm. Female aperture terminal. Ripe eggs,

possessing prolongations of middle shell,

.042-0.046 min x 0.008-0,010 mm.

Testes ellipsoidal to subglabular and placed

in tandem; anterior one 0.45-1.05 mm x 0.35—

0.45 mm and posterior one 0.50-0.91 mm x

0.34-0.43. Cement glands, two, Jong and

slender, sometimes constricted at some points.

Male aperture terminal, No genital ganglion.

like that found in male specimens of P. mugilis.

present.

Systematic position: The specimens fall with-

in the order Palaeacanthocephala Meyer. P.

coorongensis differs from P, mugilis Johnston

& Edmonds, 1947, the latter possessing a

* Department of Zoology, University of Adelaide, Adelaide, S, Aust. 5000.

te GEG ES

‘ Cal gl a et

a O- Imm .-

“ = = aa EE nF mere gt ented

Op TE ee er SE

= ee tay

~5. Pararhadinorhynchus coorongensis. Fig. 1—Introvert. Fig. 2—Row of nine hooks. Fig. 3.

Figs. 1

Male. Fig. 4.—Posterior of female. Fig. 5.—Egg,

Figs. 6-7. Pararhadinorhynchus mugilis. Fig. 6.—Introvert. Fig, 7.—Egg.

AUSTRALIAN ACANTHOCEPHALA, No, 13 , 21

longer introvert armed with 18 longitudinal

rows of 16-17 hooks per row. It also differs

from Diplosentis amphacanthi Tubangui &

Masilungan, 1937, in which the introvert bears

12 longitudinal rows of 8-9 hooks per row

and in which the Jemnisci are enclosed in a

membranous sac.

is the second acantho-

found in A. forsteri.

aldrichettae | Edmonds

P. coorongensis

cephalan species

Nevechinerhynchus

(1971) is the other.

Pararhadinorhynchus mugilis Johnston & Ed-

monds, 1947: 15.

FIGS. 6~7

The material from which the type descrip-

tion was made contained only two specimens

with everted introverts. Recently a few more

specimens in a fully extended condition he-

came available and consequently the measure-

ments given in 1947 have been rechecked. The

host was the type host, Mugil cephalus Lin-

naeus.

Introvert (Fig. 6) cylindrical. Length of

armed region 0.88-0.94 mm and width 0.16—-

0.25 mm. Sixteen to eightcen, usually 18,

longitudinal rows of 16-17, usually 17, hooks

per row, Unarmed neck, 0,15-0.25 mm long.

Ripe eggs, with polar prolongations of the

middle shell, measure 0.052-0.056 mm x

0.013-0.015 mm.

Type specimens (male and female): Austra-

lian Museum, Sydney (not the South Austra-

lian Museum, as stated by Johnston &

Edmonds 1947).

References

Epmonps, 8S. J. (1972).—Australian Acantho-

cephala No. 13. Three new species. Trans.

R. Soc. S. Aust, 95, 55-60.

Jounston, T. H. & EpMmonps, 8. J. (1947).—

Australian Acanthocephala No. 5. Trans. R.

Sac. S. Aust, 71, 13-19.

Scott, T. D. (1962).—‘“The marine and fresh-

water fishes of South Australia.” (Govern-

ment Printer: Adelaide.)

TUBANGUL, M. A, & MAsILuNGAN, V. A, (1937).—

Diplosentis amphacanthi gen, et sp. nov. an

acanthocephalan parasite in a marine fish.

Philippine Jl. Sci. 42, 183-189.

A NEW GENUS AND SPECIES OF EARTHWORM

(MEGASCOLECIDAE: OLIGOCHAETA) FROM SOUTH AUSTRALIA

BY S. J. EDMONDS*AND B. G. M. JAMIESONT

Summary

EDMONDS, S., J. and JAMIESON, B. G. M., A New Genus and Species of Earthworm

(Megascolecidae: Oligochaeta) from South Australia. Trans. R. Soc. S. Aust., 97 (1), 23-27,

28th February, 1973.

The genus Gemascolex is erected for the new species G. newmani, from South Australia. The genus

is morphologically very similar to Spenceriella Michaelsen, differing primarily in lacking the

extramural calciferous glands of the latter genus. Both genera are assigned to the tribe

Megascolecini. G. newmani is the fourth megascolecid species described from South Australia, but

of those previously described, Megascolex fletcheri Shannon is considered to be a junior synonym

of M. stirlingi (Fletcher), leaving the total number of described South Australian megascolecid

species at three.

A NEW GENUS AND SPECIES OF EARTHWORM (MEGASCOLECIDAE: OLIGO-

CHAETA) FROM SOUTH AUSTRALIA

by S. J. EpMonps* and B. G. M. JAMiEson+

Summary

Epmonps, 5S. J. and Jamieson, B. G. M., A New Genus and Species of Earthworm. (Megas+

colecidue: Oligochaeta) from South Australia. Treas. R. Soe, S. Aust. 97 (1), 23-27,

28th February. 1973.

The genus Gemuscolex is crected for the new species G. newmani, from South Aus-

tralia, The genus is morphologically very similar to Spenceriella Michaelsen, differing primar-

ily in lacking the extramural calciferous glands uf the latter genus. Both genera are

assigned to the tribe Megascolecini. G. riewmani is the fourth megascolecid species described

from South Australia, but of those previously described, Megascolex fletcheri Shannon is

considered to be a junigr synonym of M. stirlinvi (Fletcher), leaving the total number of

described South Australian megascolecid species at three,

Introduction

Three species of Megascolecidae, the only

earthworm family indigenous in Australia,

have previously been named from South Aus-

tralia. They are Megascolex stirlingi (Fletcher,

1888), placed in Perichacta by Fletcher; M,

zieizi Michaelsen, !907a; and M, fletcheri

Shannon, 1920. M. fletcher? Shannon is a

homonym, the binomen having been used by

Michaelsen, 1907a, for u distinct species from

New South Wales. Shannon’s account, though

long, is inadequate in many respects and the

type-specimens are no longer traceable, It

nevertheless conforms sufficiently with the

description of M. stirlingi 10 suggest, though

not unequivocally, that M. flercheri Shannon is

i junior synonym of M. stirlingi. The latter

species has been rediscovered by both authors

in recent collecting in South Australia ‘and

will be described in a future monograph

(Jamieson, in preparation) in which the status

of M, zietzi will also be considered.

The new species erected here has been used

for some years for undergraduate teaching and

for research in the Department of Zoology of

the University of Adelaide. It is referred to

4 new genus which is defined below. Evidence

for inehuding Megascolex stirlingi {Fletcher}

and other species in the new genus will be

deferred to the later publication.

GEMASCOLEX gen. nov.

Terrestrial. Setac numerous (more than 8)

in each segment. A pair of combined male

and prostatic pores on XVIII. Clitellum

annular, anterior to 18/19, Intersegmental

accessory genital markings present. Female

pore unpaired, midventral, in XIV. Spermathe-

cal pores anterior ta IX.

Dorsal blood vessel single. Posterior hearts

latero-ocsophageal, each arising from the sbort

supra-oesophageal vessel and from the dorsal

blood vessel. Latero-oesophageal vessels present

median to the hearts. Subneural vessel absent.

Gizzard large, anterior to septum 6/7. Oeso-

phagus lacking extramural calciferous glands.

Intestine: commencing in XVII, a low ridge

like dorsal typhlosole present; caeca and mus-

cular thickening absent. Excretory system

meronephric. Four pairs of tufted nephridia,

in II-V, their ducts (all?) enteronephric, en-

tering the buccal cavity. Succeeding segments

with astomate, exonephric, micromeronephridia

in lateral bands, Caudally with numerous

enteronephric meronephridia, each with a pre-

* Department of Zoology, University of Adelaide, Adelaide, S. Aust. 5000,

' Department of Zoology, University of Queensland. St. Lucia, Qld. 4067.

24 S. J, EDMONDS and B. G. JAMIESON

septal fiinnel, discharging into the intestine in

each segment. Testes and funnels in X and X1;

testis-sacs absent: seminal vesicles in XL and

XIL

Ovaries and Funnels in XIID, ovisucs absent

Prostates tubuloracemose: lincar, lobulated,

with axial Ittmen rhroughout which reccives

lateral canaliculi; vasa deferentia joining their

muscular ducts. Spermathecue with diverticula,

(Genuscolex, gender male, anagram of Megas-

colex).

Type species: Gemascolex hewmant sp. nov.

Distributions South Australia (see species des-

eription) .

Remarks: The closest morphological affinities

of Gemuascolex lie with two endemic Australian

genera, Spenceriella Michaelsen, 1907b, and

Oreoscolex Jamieson, 1973. The three genera

are the anly members of the indigenous Aus-

tralian Megascolecidae known to possess more

than one pair of stomate nephridia per se2-

ment, and are assienyuble to the tribe Megas-

eolecini Jamieson, 1970. Spencerfella und

Gemascolex unre especially close, as in both,

some wt least of the exudal nephridia are entero-

nephric, opening into the intestine, whereas in

Oreoseolex caudal enteronephry has been de-

duced only very questionably in the type-

species und is unknown in other species, Mul-

tiple nephrostomes and enteronephry have

been demonstrated in Spencerielle for the first

time by Jamicson (in preparation). Oreascelex

tucther differs from Gemascolex and Spen-

ceriella, among other respects, in having only

eight setae per segment.

The chief distinction between Gempscolex

and Spenceriella is the presence of extramural

ciJeiferous glands in Spencerlelfa, Both gencra

differ {rom the type-species of Megescolex in

having stomate nephridia and in their entero-

nephry (Buhl 1946). Only the non-racemose

condition to the prostates would have

separated them from Megascolex in some

former classifications,

Gemascolex newmani sp, nov,

FIG. 1

The following account refers to ihe holo-

type (H)} antl one paratype (P71); variation in

other specimens is discussed subsequently.

Length 180(P1)-234(H) mm, width (mid-

clitellar) 9 mm, number of segments 192(H):

193(P1). Colour in life: dorsal surface brown-

ish purple, ventral surface pale grey; a dark

purplish colour more noticeable at the cx-

tremities; some iridescence present. Cross sec-

tion approximately circular, Prostomium

epilobous 1/3, bisected by 4 longitudinal fur-

TOW, appearing epilanylobaus, owing to longi-

ludinul grooves continuing its lateral limits to

the first intersegmental furrow, but numerous

equally developed parallel grooves present

around the peristomium, Peristomium not

bisected ventrally though in some specimens

a mid ventral groove is more conspicuous than

others. First dorsal pore 4/5. Penchuetine.

setae of cach side more closely spaced laterally

than dorsally and ventrally: Ac slightly wider

than a’, Numbers of setac per segment 32(H)

33(PL) in XU, 26(P1)-30(H) in XX,

31(P1)-32(H) fifteen segments from the

caudal end: a lines straight, z lines irregular;

a ventral and a dorsal break in the setal

eirclet apprectiuble throughowt, Setas a and 6b,

but not ¢, absent in XVI.

INTERSETAL DISTANCES IN

Gemascnlex newmani

~ "standardized =

Te Of citeum ference

tus

tam 6

az oub gy miu aa ab ty ze

Seement NAT

Holutyre 22 08 09 62 23 78 29 32 221

Paratype 1 27 UA 1.0 6.2 28 f2 29 316 RS

Seeneut XX

Holotyne 18 O68 O09 5.6 30 60 20 ju 187

Paratsne t 2.106 13 48 3 7.2 22 42 (8.

Nephropores not externally recognizable.

Clitellum annular, not Eully developed, embrac-

ing XIV-XVIT, but some clitellar modification

present dorsally from 2/3 XII-XVUII

(=5 1/3 segments); intersegments and setae

retained but only # and & conspicuous; dorsal

pores 13/14-17/18 occhided, Mile pores a

pair in XVII, transverse slits in ab(H)} or

b(P1) and almost as wide as ah, each on a blow

transversely Oval papilla, the two papillae out-

lined by a common medianly narrowing field;

the pores 2.8-3.2 mm, 0.08-0.09 circum-

ference apart, Accessory genital markings un-

paired, midventral, transverse, clevated pads,

with lateral limits in ab, in 15/16(H, Pl),

16/16 and 19/20(H), each pad transversed

by a glandular trench corresponding with the

intersegmental furrow but not reavhing to the

ends of the pad, Female pote unpaired, mid-

ventral, in a deep transverse groove at the

anterior border of the setal annulus of XIV_

Spermathecal pores 3 pairs of sunken orifices,

concealed in intersegments 6/7, 7/8 and 8/9,

very shortly lateral of setal lincs a, 2,8=+2,9

mm, 0,09 circumference apart.

Strongest septa 10/11-12/13, very strong.

Dorsal hlood vessel single. continudus onto

the pharynx. Dorsoventral commissural vessels

NEW GENUS AND SPECIES OF EARTHWORM 25

Fig. 1. Gemascolex newmani sp. noy. A, ventral view of right spermatheca of TX (holotype); B

dorsal view of right spermatheca of IX (paratype 2); C, spermathecal pores (holotype); D.

male genital field (holotype); £, right prostate (paratype 2). Clitellum shaded. All hy camera

lucida. 9, female pore; g.m, accessory genital marking: ¢, male pore; pr.d, prostate duct;

pr.g, glandular portion of prostate; sp.amp, spermathecal ampulla; sp.d, spermathecal duct:

sp,div, spermathecal diyerticulum; sp.p, spermathecal pore. Roman numerals ate segment num-

bers,

in V-XIII; those in X—XIII forming large

latero-oesophageal hearts, each originating

from the supra-ocsophageal vessel but also re-

ceiving, at its junction with the latter, a slender

short connective from the dorsal blood vessel;

these hearts otherwise unbranched. Commis-

surals in V-IX dorso-ventral only, lacking

supra-esophageal connectives, but giving

branches to the posterior septum, gut and lateral

parietes; all commissurals, including the hearts,

yalvular. A pair of Jarge vessels originating on

the parietes in TV passes posteriorly as a pair

of large ventrolateral trunks (latcro-oesophageal

vessels), median to the dorsoventral. commis-

surals, Into TX at the posterior scptum of

which they give branches to the ventral wall

‘of the oesophagus and to the septum, Similar

paired trunks (suboesophageal vessels) present

in XI-XYIJ, closely adherent to the ventral

surface of the oesophagus and lying under its

peritoneum; no continuity demonstrable he-

tween the latero-cesophageal vessels in IX an-

™ S. 1, ERBMONDS und B. G. JAMIESON

teriorly and the suboesophageal vessels in XI

posteriorly, both pairs of vessels give a pair of

vessels to the nesuphageal plexus in each seg-

mene. Submeural vessel absent, Gizzard moder-

ately lurge, fusiform, and firrnty muscular in

Vii septum 5/6 adherent to its anterior end:

its posterior end projecting a little behind inter-

segment 7/8; the ocsophagus much narrower

in V, short and narrow in VIL dilated and

vascularized with low intermal rugac, but ne

calciferous glands, in VUI-XY, narraw and

short in XVI Intestinal origin XVIL; a low

ridgelike dorsul typhlosole commencing in

XXIF, caeca and muscular thickening absent.

Nephridia: meronephric: large paired tufts,

with very many spiral loops, in I. IL. TV and

V increasing in size pasteriad and very

large in V. Those in V and IV sending antero-

medianly thick sheaves of numerous ducts,

which loosely aggregate ay 4 composite duct

common to both pairs of tufts, the ducts pass-

ing forward (to join the lateral wall of the

buecal cavity in front of the brain, Those in

Il and I sending slender composite ducts to

the lateral walls of the buccal cavity immed-

iately behind the muuth, Nephridia in succecd-

ing segments astomate. exonephric, micro-

meronephridia: very dense transverse bands of

spital tubules, which laterally may be ¢on-

sidered to form tufts, anterior in WI, their

numerous discrete or partly aggregated ducts

Hischarzing exonephrically at the anterior limit

of the segment; some exonephric nephridia

present! pasteriorly in the segment; VIT-X each

with an anterior and a. posterior parietal band

of numerous nephridia; XI, XU and XT with

similar but rather sparse bands; XIV with

sparse anterior and dense posterior bands; XV

with Uenser unierior und sparse posterior

bands; XVI (the last oesephages! segment)

and succeeding intestinal segmests with only

anterior hands; hands dense in XIV-XVI1L.

Caudally, commencing at segment 120 (in

holotype with [92 segments), with numerous

enlarged onephridia (almost megamerone-

phridia) in each segment on the anterior wall

of the segment near to ard encireling the in-

testine, the nephridia about five deep and cach

with 4 long-slalkecl conspicuous. preseptal

funnel, the nephridial ducts in cach segment

Tunning medially as a common duct on each

side to enter the wall of the intestine anteriorly

in the segment on each side of the dorsal blood

yessel, though some individual nephridial ducts

reich the wall of the intestine independently in

the vicinity of their nephridial hodies, Concen-

tric with and external io the enlarged, entero-

nephric nephridia are parietal astomate,

apparently ¢xonephric, micromeroncphridia in

dense transverse bands. The number of cn-

larged nephridia decreases, and that of the

micromeronephridia greatly increnses, m the

last twenty or so segments.

Holandric; sperm funnels iridescent in X

and XI; Lestis-sacs absent; seminal vesacles

large lobulated sacs im XI and XII; similar.

smaller, structures on the anterior septum of

X ate of unknown function but cannot be

seminal vesicles. Ovaries (webs of large

oocytes) and funnels in XIII; vvisics nbsent,

Prostates limited to X VINE, flattened, Jobulateel

S-shaped glands with short slightly tortuous

muscular ducts joined near their ental ends by

the vasa deferentia. Penial setac absent.

Spermathecae 3 pairs, in VU, VII and IX.

diveruculun (inseminated) single, subspherical.

internally multiloculate, with a shert stalk (H,

Ph).

Field Variation: In 16. clitellate type-speci-

mens. including the holotype, a lransvetse

median genital marking is present in [5/16

and 16/17 in 9 specimens, and in 19/20) in

fO specimens, Seven of these specimens have

the Full complement. of markings, in 15/14.

16/17 and 19/20; 2 specimens have the geni-

tal marking m 15/16 only; 2 have them in

16/17 and 19/20 only: 1 has a marking in

19/20 only; und 4 have no murkings,

Murerial Exentined: Cudlee Creck, 34° 50°S_.

138°49°E,, from helow apple orchard of Mr.

G. Newman, Edmonds, August 1971—H,

PI-9; N, Maier, 21L.viti1972—PlI-s3.

Hahndorf, 35°02'S., 138°48'E.. G. Perersan,

25.viii 1972—P 70-12.

H, P2-4. deposited in the Australian

Museum. Sydney; PL. 5, British Muscum

(Natural Histury); P6. 7, South Australion

Mailscuum; P8—-12 famieson collection,

Remarky: Material used in undergraduate

stadies and not retained cannot be designated

type-material but. nevertheless, variation in it

may be noted. In 50 specimens the length was

200-271) mim; the width was 7-9 min generally

but 8-11 mm in the region of crop and gizzard.

The clitelum embraced XIV-XVII hui some-

times included part of MII and of XVIIL

Numbers of spetmathecal pores and location

of the male pores and of the female pore were

constant. Accessory genital markings, when

present, were usually at 15/16, 16/17 and

19/20, The iitestine usutaily began. iy XVI,

a condition also noted in some nf the type-

NEW GENUS AND SPECIES OF EARTHWORM 37

specimens. The flattened S-shaped form of the

prostales was constant, The supra-oesophageal

vessel occupied VII-X1V, ramifying on the

oesophagus at each end, In one hundred speci-

mens the number of segments was 155-198,

The course of the suboesophageal blood

vessels has not been unequivocally determined

and, with that of the latcro-parietals, requires

further examination. The structures resembling

seminal vesicles anteriorly in X do not show

spermato-genests in serial sections, whereas the

seminal vesicles in XI and XII do.

Gemascolex newmani is distinguished from

the equally large Megascolex stirlingi, so fai

as it is described by Fletcher, 1888, in (a)

location of the spermathecal and male pores

in ab lines whereas in M. stirlingi they are

markedly more lateral, in setal lines 6 and be-

tween setal lines 3 and 4 respectively; (b) the

unpaired instead of paired accessory genital

markings and their forward extension to inter-

segment 15/16; (c) the S-shaped, not straight,

prostates and in other respects.

Noteworthy differences from MM. zierzi, as

described by Michaelsen, 1907a, are (a) the

more median location of spermathecal and

male pores, (b) location of the male pores well

lateral of paired accessory genital markings in

M zietzi, (¢) presence of further paired mark-

ings on the anterior border of the male poro-

phores in the latter species; (d) restriction of

the prostates to XVIII and their S-shaped

form: (c) the subspherical sessile spermathe-

cal diverticulum of newsani contrasted with

the very Jong tortuous tubular diverticulum of

M. zietzi.

Acknowledgements

The authors thank Mr, G, Newman for per-

mitting collection of the new species from his

property and Mr. G, Peterson and N. Maier

for procuring additional material. This work

was carried out during tenure of ARGC and

URG grants,

References

Bani, K. Ny (1946).—Studies on the structure,

development, and physiology of the nephridia

of Oligochaeta. Part VII. The enferonephric

type of nephridial system in carthworms be-

longing to three species of Megusvolex

Templeton and three. species of Travoscolides

Gates (Meguscolides McCoy), Q. JI microse:

Sei. 87, 45-60,

FLeTcHer, J. J. (1888)—Notes on Australian

earthworms, Part II, Proc. Linn. Soc, NSW.

2, 375-402.

Jamirson. B. G. M. (1970).—A review of the

megascolecoid earthworm genera (Oliza-

chasta) of Australia, Part 1—Reclassification

and checklist of the megascolecoid genera of

the world. Prov. R. Soe. Od B2(6), 75-86.

JAMizson. B. G. M,. (1973).—Earthworms

(Megascolecidac: Oligochueta) from Mount

Kosciusko, Australia. Rec. Ast. Mus. (in

press.) .

MICHAELSEN, W. (1907a).—-Oligochaeten von Aus-

tralien. Abh. Geb. Naturw., Tamburg 19(1),

1-25.

MICHAELSEN, W. (19076) —Oligochaeta in: Die

Fauna Sidwest-Australieny 1(2), 177-232.

SHANNON, J. H. (1920).—On the structure of 2

new species of carthworm from South Aus-

tralia, Megascolex fletcheri. Proc, R. Soc.

Viet. 32, 301-313, Pl. XXVII-XXXI

AERIAL DISPERSAL OF ADULT CARDIASPINA DENSITEXTA

(HOMOPTERA:PSYLLIDAE) IN SOUTH AUSTRALIA

BY T. C. R. WHITE*

Summary

WHITE, T. C. R., 1973. Aerial Dispersal of Adult Cardiaspina densitexta (Homoptera:Psyllidae) in

South Australia. Trans. R. Soc. S. Aust. 97 (1), 29-3 1, 28th February, 1973.

Living adult C. densitexta were captured at 152 m and 305 m above the ground in the vicinity of

Keith, South Australia during the spring. This finding supports the hypothesis that the adults of the

spring generation generally function as the effective dispersive stage in the life cycle of this insect.

AWRIAL DISPERSAL OF ADULT CARDIASPINA DENSITEXTA (HOMOP-

TERA: PSYLLIDAE) IN SOUTH AUSTRALIA

by T. C. R. WuiTeE*

Summary

Wurrr, T. C. RK. 1973, Aerial Dispersal of Adult Cardiaspina densitexta (Homaptera:

Psyllidac) in South Australia. Trans. R. Sac. §. Aust. 97 (1), 29-31, 28th Febrmary_ 1973.

Living adult C. densitexta were captured at 152 m and 305 m ahove the ground in the

vicinity of Keith, South Australia during the spring. This finding supports the hypothesis that

the adults of the spring generation generally function as the effective dispersive stage in the

life cycle of this insect.

Introduction

Clark (1962) concluded as a result of his

obseryations and experiments with adults of

Cardiaspina albitextura Taylor that emerged

in the autumn, that they tend not to disperse

far from their point of origin, and that there-

fore this is “ . not a strongly dispersing

insect.”

Studies of the closely related Cardiaspina

dénsitexta Taylor (White 1970a) suggested

that although this seemed to he true of the

generation of adult C. densitexta that emerged

in the summer and autumn, it did not seem to

be true of the generation that emerged in the

spring. During summer and autumn, trees that

were isolated from the established infestations

were rarely colonized, Also at this time of the

year. adulis seemed to show great “reluctance”

to leave the foliage on which they had devel-

oped, On the contrary, during spring it was

commonplace for isolated trees to be colonized

quickly. Also direct observation of the be-

haviour of adults at this season of the year

showed that they had a strong tendency to

fly up and away from the foilage on which

they had lived as nymphs.

These observations led to the hypothesis

that C. densifexta exhibits two types of seasonal

behaviour: (1) non-dispersive, serving to con-

Sentrate summer and autumn adults—and sub-

sequent egg-laying—on favourable foilage; (2)

dispersive, serving to distribute the adults

emerging in ihe spring away from depleted

foilage ind increasing the chance of some of

them finding fresh foilage.

This would suggest that the adults thai

emerged in the spring were the effective dis-

persive stage in the life cycle of C. denvirexta,

most probably in the manner proposed by

Lewis & Taylor (1965). Their analysis of

many aerial samples demonstrated that “high

altitude and long distance migration is very

highly correlated with flight by day and small

size.”

Such an hypothesis presupposes that adults

of C. densitexta which emerged in the spring

were present high in the air where they would

be widely and randomly dispersed by air cur-

rents and winds. In 1964 an attempt to demon-

strate this was unsuccessful. By the time a

suitable technique had been developed, num-

bers of C. densitexia had fallen to very low

levels, reducing to near zero the probability of

catching the few individuals that might have

been present in the aerial plankton,

This paper Treports a second attempt to

catch airborne adult C. densitexta at a time

when they were abundant.

Materials and Methods

Nets mounted on a steel ring 38 cm in

diameter were towed from the wing of a

Cessna 172 aeroplane flying at 1352 and 305 m

above the ground. Details of the construction

* Department of Zoology, University of Adelaide, Adelaide, S. Aust. 5000.

Present Address; School of Natural Resources, University of the South Pacific, Sova, Fiji,

30 TCR,

of the nets and the cing, and of the method of

Operaling, were described previously (White

1970b).

All samples were of 15 minutes duration.

Euch net was released when the aeroplane had

levelled off at the required height and was

cruising at 121-131 km/h. Height and speed

were maintained as accurately as possible for

the duration of each sample.

All nets were kept sealed in plastic bags

until immediately before being used, At the

completion of each sample a knot wus tied in

the net before it was detached from the ring

and resealed in w plasti¢ bag. All bags were

returned to the laboratory before being opened

and the nets immersed in 70% alcoho! before

the knots were untied.

All collections were made over a relatively

amall area between Keith and Willalooka jin

the southeast of South Australia (White 1970b,

fig. 2), At the time the host plants (Eucalyp-

ius fascieulosian Fv.M.) in this locality were

carrying w moderate to high population of C.

densitexta, wind ahout 50%. of the adults had

emerged.

Results

Forty-one samples {Table 1) were collected

during, five days, thirty at 152 m and eleven at

305 m, Twenty cight contained adult C. den-

xitexia, the catch varying from one to nine

per sample at 152 m, and one to five per

sample at 305 m, A total of 60 adults were

caught. there being approximately equal num-

hers of males and females, Several were ob-

served crawling around in the nets after these

had been placed in ptastic hags.

TABLE |

The number of adult C_ densitexta captured

No. of Aln-

Date Samples — tude a 9 + Fatal

Lexi7t LL(7j* [52m 5 5 1 oul

2.x1.71 77) 1S2m fi 8 2 16

3x17] §(3) 132m 2 2 1 3

VL .xi.7t 4(3) [52m 4 5 2. al

4(4) wim — 2 ] 3a

12.xi.71 73) 305 m 5 of 3. 614

Total 41(28) _— 22 28 #10 60

* Number of samples containg C. denstrexta in

parenthesis.

+ Damuged individuals lacking an abdomen,

A net with a diameter of 38 cm, pulled

through the air at a mean speed of 126 km/h,

would sift 221 m* of air per minute—3319 m!

in a 15 minute sample. But because of the

WHITE.

“cushion” of air formed in Front of the net. at ix

improbable that this volume of air would have

passed through the net, Much of it would have

been deflected around the sides of the net, No

attempt was made to assess the “effective”

diameter of the nets—it. may well have been

no more than 2.5 om to 5 ¢m but if a conser-

vative 7.5 em miurgin is deducted to whow for

deflection an clfevtive diameter of 23 ¢m re-

mains. Then 1188 m® of air would have been

sampled in 15 minutes.

A 152 m high block of air ubove a hectare

of jand contains 1,520,000 m* of air, at 305

m, 3,050,000 m*, Tf the adult psyllids were

distributed wt random through this air, the

sampling indicated densities of from about

1,300 to 11,500 per hectare to a height of 152

m and trom 2,500 to 12,800 per hectare to

305 m.

Discussion and Conclusion

The number of unknowns makes any

uttampt to quantify the density of adult psyllids

in the aerial plankton unrealistic. Quite apart

trom the problem of the effective size of the

sampling unit, it is likely that the distribution

of ait-borne psvilids was far from random.

The time of day, ambient temperature, wind

speed and the extent and duration of the warm

au “thermals” rising from the ground would

all have contributed to a patehy and variable

distribution, both vertically and horizontally,

Almost certainly this sampling underesti-

mated the number of these insects in the air

over any area of land, But equally certainly it

demonstrated that there were very many of

them carried to considerable heights above

the trees on which they emerged; sufficient to

ensure that they would have been scattered

over many square km of land, As the air

cooled each evening and they returned to earth.

relutively few of them would have been for-

junate enough to Jand on a suitable host plant.

But the few that did would have survived, and,

with their huge capacity for increase. soon

utilized the available food.

The evidence from this sampling. combined

with that previously reported {White 1970a),

demonsteated that the adults of C. densitexta

that emerge in the spring are the means by

which this species of psyllid i widely and

effectively dispersed.

Other records of adult psyllids captured high

in the air (Glick 1961; Freeman 1945, Hardy

AERIAL DISPERSAL OF CARDIASPINA DENSITEXTA 31

& Milne 1938) and as far as 298 km from the

nearest land (Yoshimoto & Gressitt 1963;

Harrell & Yoshimoto 1964) suggest that this

method of dispersal is common within the

Psyllidae.

Acknowledgements

A grant from the Endowment and Scientific

Research Fund of the Royal Society of South

Australia made it possible for this sampling to

be carried out.

I am grateful to Gordon Burnard for

arranging the hire of the aeroplane from the

Pinnaroo Aero Club and for his and Barry

Browne’s patient and skillful piloting. To Joan

Burnard my thanks for her hospitality and for

allowing her kitchen to be converted into a

temporary laboratory,

References

CLaRK, L. R. (1962).—The general biology of

Cardiaspina_ albitextura (Psyllidae) and its

abundance in relation to weather and para-

sitism. Aust. J. Zool. 10, 537-86.

FREEMAN, J, A. (1945).—Studies in the distribu-

tion of insects by aerial currents, The insect

populations of the air from ground level to

300 ft. J. Anim. Ecol, 14, 128-54.

Guicx, P. A. (1961).—Airborne movement of the

Pink Bollworm and other arthropods. Tech,

Bull. U.S. Dept, Agric. 1255, 1-20.

Harpy, A. C. & Ming, P. S. (1938).—Studies in

ihe distribution of insects by aerial currents.

Experiments in aerial tow-netting from kites.

J, Anim. Ecol. 7, 199-229,

Harrei, J. C. & Yosuimoto, C. M. (1964).—

Trapping of airborne insects on ships on the

Pacific, part 5. Pacific Insects 6, 274-282.

Lewis, T. & Taytor, L. R. (1965).—Diurnal

periodicity of flight by insects. Trans. R.

ent. Soc, Lond, 116, 393-479.

Waite, T. C. R. (1970a).—Some aspects of the

life history, host selection, dispersal and

oviposition of adult Cardiaspina densitexta

Comaninrs = Feyiligar). Aust J. Zool. 18,

105-17,

Waite, T. C. R. (1970b).—Airborne arthropods

collected in South Australia with a drogue-

net towed by a light aircraft. Pacific Insects

12, 251-259.

Yosutmoto, C. M. & Gressirr, J. L, (1963).—

Trapping airborne insects in the Pacific-

Antarctic area, 2. Pacific Insects 5, 873-883.

LIFE HISTORY, LARVAL MORPHOLOGY AND RELATIONSHIPS OF

AUSTRALIAN LEPTODACTYLID FROGS

BY G. F. WATSON AND A. A. MARTIN®*

Summary

WATSON, G. F. and MARTIN, A. A., 1973. Life History, Larval Morphology and Relationships of

Australian Leptodactylid Frogs. Trans. R. Soc. S. Aust., 97 (1), 33-45, 28th February, 1973.

Disagreement exists regarding the phylogeny, relationships and classification of Australian

leptodactylid frogs. Analysis of their life history patterns indicates that one of the present two

subfamilies, the Myobatrachinae, is a close-knit natural group, whereas the other, the Cycloraninae,

is more heterogeneous. In particular, the genus Cyclorana does not conform with the cycloranines,

and in terms of life history has strong affinities with the Hylidae. No close relationship between the

Myobatrachinae and the Cycloraninae is evident from life history data.

LIFE HISTORY, LARVAL MORPHOLOGY AND RELATIONSHIPS OF

AUSTRALIAN LEPTODACTYLID FROGS

by G. F. WatTson* and A. A, MartTIn*

Summary

Wwarsan, G, PF, and Martin, A. A., 1973. Life History, Larval Morphology and Relationships

of Australian Leptodactylid Frogs. Trans, R. Soc. S. Aust., 97 (1), 33-45, 28th February,

1973,

Disagreement exists regarding the phylogeny, relationships and classification of Australian

leptodactylid frogs. Analysis of their life history patterns indicates that one of the present

two subfamilies, the Myobatrachinae, is a close-knit natural group, whereas the other, the

Cycloraninae, is more heterogeneous. In particular, the genus Cyclorana does not conform

with the cycloranines, and in terms of life history has strong affinities with the Hylidae. No

close relationship between the Myobatrachinae and the Cycloraninae is evident from life

history data.

Intreduction

In the first substantial monographic study of

Australian anurans, Parker (1940) divided the

Australian representatives of the family Lepto-

dactylidae into two subfamilies: Cycloraninae

and Myobatrachinae. The major characters

used to define the twa groups were the struc-

ture of the tongue, hyoid apparatus, larynx

and thigh musculature, Martin (19672) noted

that biological characteristics, particularly life

history, were broadly consistent with Parker’s

division, Lynch (1971), using a complex of

morphological, osteological and ecological

characters, substantiated Parker's taxonomic

interpretation; he further divided Puarker’s

Cycloraninae into two tribes, Cycloranini and

Limnodynastini. Tyler (1972a) investigated

the superficial mandibular musculature and

vocal suc struciure of Australian leptodacty-

lids, and came to conclusions similar to those

of Parker and Lynch, with one important ex-

ception, Tyler found that Cyclorana Stein-

dachner did not conform with either the

Cycloraninae or the Myobatrachinae; and he

questioned its familial disposition, noting that

it shared some characters with the amily

Hylidae.

The generic classification of Australian

Jeptodactylids has undergone considerable

modification since Parker's work. Heleioporus,

as recognized by Parker, was divided into two

genera, [eleioporus Gray and Neobarrachur

Peters. by Main (1957a); and the new genera

Kyarranus Moore, 1958 and Taudactylus

Stranghan & Lee, 1966 have been erected.

Tyler (1972b) removed Crinia darlingtoni to

# new genus, Assa. Blake (in press), using a

polythetic mumerical approach; finds that

Crinia is divisible into three gencta, and group-

ings corresponding to these genera are used

here, They are referred to as the Crinia has-

well’ group (including C. haswelli and C.

georgiana); the Crinia laevis group (including

C, Jaevis, C. leai, C. lutea, C. rosea and C.

victoriana); and the Crinia signifera group (in-

eluding all other species of Crinia). Blake (in

press) also finds that Mezacrinia Parker does

not warrant separation from Pseudophryne

Fitzinger and he intends to synonymise these

two genera; hence they are not treated separ-

ately here. The current composition of the

Australian leptodactylids is shown in Table 1.

The present contribution summarizes the

available data on the life histories and larval

morphology of Australian leptodactylids. Such

information is useful from two points of view,

First, life history stages provide morphological

characters independent of those exhibited by

+ Department of Zoology, University of Melbourme, Parkville. Vic. 3052.

a4 G. F. WATSON and A, A, MARTIN

adults, and can therefore be uscd to test

phylogenetic relationships based on studics of

adults (such gs the suggested hylid affinitics

of Cyclorana), provided that care is taken

to recognize convergence (Inger 1958; Griffiths

1963}. Second, life history is an indicator of

geferal adaptive ecology, and generic defini-

tion is currently based on ecological as well as

morphological characters (Mayr 1969). Inger

(1958) has demonstrated the utility of life

history data in anuran classification at the im-

frafamilial levels, and this approach was used

by Martin & Watson (1971) in an analysis. of

the family Hylidae. Although Lynch (1971)

took life histories into account in his analysis

of the leptodactylids, mast of his dats on Aus-

trilian forms as derived from the literature,

and is often inadequate or erroneous.

TABLE |

fnfrafamiltal classifications of Astralian

leprodavtytids,

Adelotun

Kyarramis q

Lechriodus Linney

Lim nodynuntcs: fork 197) Subsamii

" ft

Philovin Cycloraninae

Tribe |

; F Yas

Meleigporus | Bates

Subfamils

Cyeloruninac

(Tyler 19729)

Mixophyer Tribe

Neobatachut Cycloranini

Notaden | cad 171)

Cyclorans

Crinia laevis group

Crinia signitera group

Glavertia

Myobarrachus

Peeudophryne

Taudactylus

Uperoleia

Subfamily

Myobatruvbinar

(Varker 1940; Lyaet 197t,

Asia

Crinia haswelh sroup |

f Teler 19720; Make in prose)

Material and Methods

Material representing all but four of the 17

venera of Australian leptodactylids has. been

examined, The four gencra not studied are

the cycloranine Noteden Gunther ahd the

myobatrachines Awsa Tyler, (lanertia

Loveridge and Myehatrachuy Schlegel. For

these genera data have been drawn from the

literature. One or more species of each of the

other genera have been examined; all obser

vations mot supported by 4 reference are

original. In some cases (e.2, Limnoadynastes,

the Cvrinia signifera group) enough species

have been stucbed to be fairly confident that

the limits of intrageneric vartalion in life his-

tory have been detected; in others (¢,g. Tanda

tylus), only one species hus been examined

and the present account may therefore not be

characteristic of the genus.

Identity ul life history stages was established!

hy rearing eges of known parentage, or by rais-

ing to metamorphosis a portion of each tuilpele

sample, The only exception is Taudacrylus,

where identification of the larvae is based on

the fact that they were collected at the type

locality of 7. diurnus, and are distinct fram

the larvae of any other anuran known to in-

habit the area.

Although data on numerous characters were

assembled, five major feutures of the life

history showed consistent variation and were

employed in our analysis, These features, inost

of which are illustrated in Martin (1965), are:

(1) Type of egg mass: whether foamy or

nat.

(2) Larval development: whether terres-

trial or aquatic.

(3) External gills: whether present or ab-

sent in embryonic development,

Number of rows of teeth in the upper

lubium of the larval mouth: whether

nonc, two, or more than twa.

Disposition of labial papillae in the

larval mouth; whether completely sur-

rounding the mouth disc (na gaps), or

with an anterior gap, or with both .an-

terior and posterior zaps.

One additional character commonly em-

ployed in larval descriptions—whether the

anus is median or dextral—is included for the

sake of complcteness, but in many groups 7

is too variable (even within genera) to be use-

ful in the analysis of affinity (Lee 1967; Lynch

1971). The larval morphology of each genus

is Wustrated by drawings of the indpoles of

one or more species in lateral view, and of the

larval mouth dises, Larvae between stages 3f)

und 38 of Giosner (1960) were used for illu-

stration. Where material was avilable For

several species in a genus, the specics selected

for illustration and description is generally

one which has not been considered in our pre-

vious publications (e.g. Martin 1965, 19674),

The description relers to the species illustrated,

and variations in other species are noted.

Drawings were mude with the aid of a stereo-

scopic microscope, using photographs, a

cameta lucida, or an ocular micrometer and

squared paper.

(5)

Survey of Life Histories

Adelotus Ogilby

Species examined: A. Arevis, Trani Mt_ Nebo.

Old.

The egg mass is foamy und is deposited In

standing or flowing water, development 4s

AUSTRALIAN LEPTODACTYLID FROGS

Sie me,

Cree

ea epE ITS os,

C Pepa a ee

ey my

S97 > pcean,

SPER

Fig. 1, Left lateral view of larvae of: A, Adelotus brevis; B, Lechriodus fletcheri; C, Kyarrunus

sSphagnicolus;

45mm,

aquatic. The eggs lack pigment and have a

diameter of 1,7 mm (Martin 1967a). There

are no external gills. The anus is dextral, and

the larva has an unspecialized body form (Fig.

1A). There are three upper and. three lower

rows of labial teeth (not two upper and three

lower as stated by Lynch 1971), and a gap in

the labial papillae along the anterior margin

of the mouth disc (Fig. 2C),

Adelotuy is a monotypic genus.

Kyarranus Moore

Species examined: K- sphagnicolus, from Point

Lookout, N.S.W.

The foamy egg mass is placed out of water,

in damp sphagnum moss, and the larvae do not

feed, though they may become free-swimming

(J. M. de Bavay, pers. comm.). Small external

gills are present, The larva has a relatively long

tail and broad fin; the anus is median (Fig.

1C). The mouth parts are reduced, with well-

developed jaws but no labial teeth; the papillary

border is broken anteriorly (Fig. 2D).

The life history of K. loveridgei is very

similar (Moore 1961).

BD, Limneodynastes interloris; E, Philoria frosti, In each case the bar represents

Lechriodus Boulenger

Species examined: L. flercher?, ftom Cunning-

ham's Gap, Qld.

Development is aquatic, often in highly

ephemeral situations. The egg mass is foamy

and the ovidiameter is about 1.7 mm (Martin

1967a). Long, filamentous external gills are

present. The larvae (Fig, 1B) are carnivorous

and development is rapid (Moore 1961), The

anus is median. The mouth disc (Fig. 2A)

has large jaws, and six upper and three lower

rows of labial teeth. Labial papillae are absent

from the anterior margin of the mouth disc.

Lechriodus is incorrectly described by Lynch

(1971) as having only two upper labial tooth

rows,

L. flercheri is the only representative of the

genus in Australia, but there are several species

in New Guinea (Parker 1940).

Limnodynastes Fitzinger

Species examined: L. dumerili, L. fletcheri, L

interioris, L. peroni, L. salmini, L. tas-

maniensis, L. lerraereginae.

36 G. F. WATSON and A. A. MARTIN

. Panis

~™

psy ree

‘ust tle eV,

we Er alee ge Oh

veel apnea aytyner en

ee eee

a eg

com a UA

~ ah

‘aye

" ven eH Ye nny r

to a

x 1 ee Nara wh a

we bingy SILAS

VERA VEY ITER S

PIAVIL ERAN

—oe

Nanya NTE

Fig. 2. Laryal mouth discs of: 4, Lechriodus flétcheri: B, Limnodynastes interioris; C, Adelotus brevis;

D, Kyarranus sphagnicelus; FE, Philoria frasti. In each case the bar represents 1 mm,

Species deseribed: L. inrerioris, from Boree

Creek, N.S.W.

The egg mass is large and frothy, and is

deposited in water among vegetation, under

logs or rocks, or in water-filled burrows in

stream banks (Martin 1967a); development is

aquatic. The ovidiameter is about 1,7 mm.

Externat gills are small and unbranched. ‘The

larva (Fig. 1D) has a generalized body form;

the anus is median, There are six upper and

three lower rows of labial teeth, and Jabial

papillae suzround the mouth disc except for

the anterior margin (Fig, 2B).

This life history pattern seems fairly con-

stant throughout the genus. In southern Vic-

torign and Tasmanian L. peroni, the eggs are

unpigmented (Littlejohn 1963a). Egg counts

range from 1,100 in ZL. tasmaniensis to 3,900

in L. dumerifi (Martin 1967a), All species

have at least 4, und usually S—6, rows of teeth

in the upper labium.

Philoria Spencer

Species cxamined: P, frosti, from Mt, Baw

Baw, Vic.

AUSTRALIAN LEPTOGDACTYLID FROGS 37

ET gl,

fig SH

Fig. 3. Left Jateral view of larvae of: A, Heleioporus australiacus; B, Cyclorana cultripes; C, Mixe-

phyes balhus; D, Neobatrachus pictus, Tn each case the bar represents 5 mm.

The frothy egg mass is placed in damp

sphagnum near water; the eggs are unpig-

mented and have a diameter of 3.9 mm (Liftle-

john 19636). Small external gills are present.

The Jarvae may be free-swimming but

apparently do not feed, The anus is median

and the tail fin large in proportion to the body

(Fig. 1B). The mouth has well-developed

jaws, and papillae on the Jateral and posterior

margins of the disc, but labial tecth are absent

(Fig. 2B).

Philoria is a monotypic genus.

Heleiaporus Gray

Species examined: H. awstraliacus, ftom 12

km 'S. of Walhalla, Vie.

The eggs are unpigmented and measure 2.6

mm in diameter; egg counts of four masses

ranged from 775—1,239 eggs. The egg mass

is foamy and is deposited in standing or flowing

water concealed in vegetation or in burrows;

development is aquatic. The external gills are

prominent. The Jarvae (Fig. 3A) are un-

specialized, with a median anus. The mouth

disc has six upper and three lower rows of

{ahial teeth, and an anterior gap in the papil-

lary border (Fig. 4A).

lee (1967) has described the lite histories

of the five Western Australian species of

Heleivporus. In these, the cggs (mean ovi-

diameters 2.6—3,8 mm; mean egg counts 160—

480 eggs) are laid in dry burrows which are

later flooded, and the larvae undergo aquatic

development. The anus muy be median of

dextral. and there are 5-6 rows of teeth in the

upper Jabium-

Mixophyes Gunther

Species examined; M. halbus, M. fasciolatus.

Species described: AM]. balbus, from Point Look-

out, N.S.W.

The cggs (ovidiameter about 2.8 mm) ure

pigmented and are laid in clusters on rocks or

gtavel near the edge of flowing streams, Each

egg has a distinct separate capsule, and the

mass 3s not frothy, External gills are present.

Development is aquatic, and the larva is a

large and powerful lotic form (Fig, 3C). The

anus is dextral. The mouth disc has a com-

plete papillary border, and six upper and three

lower tows of jabial teeth, There are also 5-6

lateral rows on each side near the angle of the

jaw (Fig. 4B). The hind limbs develop in a

membrgnous sac and are not visible until late

in development.

The life histories of Mf. balhus and M-

fasciolatus appear to be essentially identical

(Martin 19674). Details of life history in the

other two members of the genus are not

recorded,

Neobatrachnus Peters

Species examined; N. centralis, N. pictus.

Species described: N. pictus, from Savernake,

N.S.W.

The eggs are pigmented and about 2.2. mm

in diameter. They are Jaid in strings of jelly

wound among submerged vegetation in stand-

ing water, and development is aquatic. Small

external gills are present. The larvae are active

swimmers with relatively plump bodies.and short

§ G, F. WATSON

—_——> 7

SSP mht ee

Teac ee Cr <

nm al Arnaut sen aie

POLLEN

sry naan nen oo

and A, A. MARTIN

Seti,

n Uh Sener a,

yltss f

atl

RA Usyas 14-4

Peery yan?

acl ; re

4 ee

a gabtirae ing

Fig. 4. Larval mouth discs of: A, Heleioporus ausiraliucus; B, Mixophyes halbus; C, Neobatrachts

pictus; D, Cyclorana coltripes. In each case the bat represents 1 mm.

jails (Fig. 3D). The anus is median or slightly

displaced to the right. Papillae are absent from

the anterior margin of the mouth dise, and

there ate three rows of teeth in each labium

(Fig. 4C). The jaws are very robust, presum-

ably reflecting the fact that the larvae feed by

ingesting large fragments of plant and insect

material (M. J. Tyler, pers. comm.).

In castern populations of N. centralixs the

eygs huve discrete capsules and are laid sep-

arately or in loosely adherent clumps. The

three endemic Western Australian species lay

their eggs in Jong strings (Main 1965, 1968).

Notaden Gunther

Species deseribed: N. richollsi, from Munka-

yarra, W.Aust.

This account is taken from SJater & Main

(1963). The eggs are 1,3 mm in diameter and

pigmented; they are laid in temporary pools

and development is aquatic. The form of the

egy mass, and whether or not external gills

develop, are not recorded. The anus is median.

There ate three upper and three lower rows

of labial teeth, and papillae extend around the

sides and back of the mouth disc.

Vhere is no information on record concern-

ing the life history of the other members of

this genus, N. hennetti and N. melanoscaphus.

Cyclorana Steindachner

Species examined: C. australis; C, cultripes, C,

platycephalis.

Species described: C,

Creek, N.T.

Development is aquatic, "The eggs are small

and pigmented and are Jaid in clusters, without

distinct separate capsules, in water (Main

3965), Embryonic development is not re-

corded, The larva (Fig. 3B) has a distinctive

acuminate tail tip; the anus is dextral, though

often only slightly displaced from the midline.

There are two upper and three lower tows of

labial teeth, and papillae occur along the

lateral and posterior margins of the mouth

disc (Fig. 4D).

The eggs and larvae of C, platyeephalus,

and the larvae of C. australis, are. similar to

those of C, cultripes. No data are availible for

other species in the genus.

culrripes, from Pine

AUSTRALIAN LEPTODACTYLID FROGS wy

eer

Fig. 5. Left lateral view of larvae of: 4, Crinia kaswelli; 2, Psendophryne corrobaree: C, Crinia leeviy:

DBD, Crinia rasea. In each case the bar represents 5 mm.

Assa Tyler

Species described: A. darlingtoni, ‘rom the

Macpherson Range. Qld.

The eggs are unpigmented and average 2.5

mm in diametet. Oviposition and embryonic

development are not recorded. The larvae de-

Velop in a brood pouch of the male, but details

of their morphology have nor been described

(Straughan & Main 1966).

The genus A'vsa is monotypic.

Crinia Tschudi

‘CRINIA HASWELLI group

Species examined: C. Aaswelfi, from 7 km W.

of Orbost, Vic,

The eggs measure about 2 mm in diameter

uid are pigmented, with distinct individual

capsules. They are laid in water and develop-

ment js aquatic. External gills are absent. The

larva (Fig. 5A) is a specialized nektonic form

with high fins. The aous is dextral. The tadpole

appeurs to feed largely on plankton, The

mouth has two upper and two lower rows of

labial teeth, and a single row of papillae bor-

dering its lateral and posterior margins (Fig.

6A).

The Western Australian C. georgiana, the

only other member of this group, has 4

markedly different pattern of development

(Main 1957b, 1965). The eggs ate latd in

permanent streams and soaks. Larvae are of

the lotic type, being flattened, and with long,

slender tails (see Main 1957b, Fig. 2a).

There are three rows of teeth in egch labium,

and the papillary border has both anterior and

posterior gaps.

CRINIA LAEVIS group

Species examined: C. laevis, C. resea, C. vie-

7oriand,

Species described; C. lJaeviy, from Wynard,

Tas, and C, resea, from Pemberton, W.A,

In C. leevis the eggs are pigmented, about

3 mm in diameter, and with discrete capsules-

They are laid in concealed sites on Jand. and

embryonic development is intracapsular. There

are no external gills. After the eges ure flooded

by winter rains the larvae (Fig. 5C) hatch

and undergo aquatic development. The anus

is dextral, The mouth has two upper and three

lower labial tooth rows, and papillae are absent

from the unterior and posterior margins of the

mouth dist (Fig. 6C).

Tn C, rosea the eggs are unpigmented and

have a diameter of 235 mm (Main 1957b),

The entire development takes place on Jand,

and the larva (Fig. 5D) is highly modified,

with no mouth disc (the mouth is a simple

slit), a large yolk sy¢ and an elongate tail, The

anus. is. median,

All members of this species group have one

or other of these modes of development: the

C. Inevis pattern is shared by C. leai and C.

victoriana, and the C. rosea pattern by C’.

lutea (Litlejohn & Martin 1964; Main 1957b,

1963).

CRINIA SIGNIFERA proup

Species examined: C. parinsignifera, C. riparia,

C. signifera, C. sloanei, C.. tasmaniensix,

Species described: C. parinsignifera, from 6

km §.E. of Wandong. Vic.

The eggs are 1.3 mm in diameter, pig-

mented, and with distinct individual capsules.

40 G. F. WATSON and A. A. MARTIN

é 1) Z os

weer

ele 73 2

re pal o

in to

EY Nui ity

“hh v Se Twa a ut ~

wy Sai i

Ag * - # nN aa

h. wun coo tr wl a0 ~

wo ee ec ass

} petra

‘Ry

Mig

oj uy vein in rl fo

ANANTH

Ming

Won

NAO

Dr.

Aa Ty

: o

Se ange ve)

Ss ne Rowny oN

S Od " eo a)

} A

. ~—S

a SS

‘ m “ai 4 S

ay i me >

yp Ln Se 1 yu yr

Fig. 6. Larval mouth discs of: A, Crinia haswelli; B, Pseudophryne cerroberce: C, Crinia laevis; D.

Crinia parinsignifera; E, Taudactylus diurnus; F, Uperoleia marmorata, In euch case the bar

represents 1 mm,

AUSTRALIAN LEPTODACTYLID FROGS 4i

Ovipasition und developmient are aquatic, Ex-

ternal gills are absent. The Jarva (Fig. 7A) is

unmodified, with a dextral anus. The mouth

has an incomplete papillary border, with both

anierior and posterior gaps, and there are two

upper and three lower tows of labial teeth

(Fig. 6D).

There is little variation in life history in this

group. The same basic pattern is shared by

C. glauerti, C. ingsignifera, C. pseudinsignifera;

C. svbinsignifera and C. tinnula (Main 1957b,

1965; Straughan & Main 1966). In C. fas-

maniensis and C. riparia the eggs are larger

(ovidiameters 1,96 and 2.27 mm _ respec-

tively), and the latter has terrestrial. oviposition

und a lotic type of larva (Martin 1967b; Little-

john & Martin 1965).

Glauertia J overidge

Species described: G. russelli, from Western

Australia.

The cggs have a diameter of about 1.4 mm

atd are laid in water: development is aquatic

(Main 1968). No other details of the life his-

tory have been recorded, and the life history of

G_ miohergt is entirely unknown.

Myobatrachus Schlegel

Species described: M. gouldi, from Western

Australia.

The cggs reach a diameter of 5,5 mm (Wat-

son & Saunders 1959). No other life history

data are on record. but. from the large egg

size and general adult ecology it is very

probable that development takes place on land

(Main 1968).

Myobatrachus is a monotypic genus.

Pseudophryne Fitzinger

Species examined: P. australis, P. bibreni, P.

curiacea, P. correbayee, P. dendyi, P,

remimarmorata.

Species described; P. carreboree, from Mt.

Ginini, A.C.T,

The eggs are pigmented and have a diameter

of about 3 tum. They haye firm, discrete

capsules and are laid on land, in tunnels in

sphagnum. Embryonic development occurs

within the capsule and there are no external

gills. The larvae (Fig. 5B) develop in water.

The anus is dextral and the mouth has two

upper and three lower rows of Jabial teeth.

There are gaps in the papillary border at both

the front and reat margins of the mouth dise

(Fig. 6B).

This pattern of life history—large eggs laid

on land, intracapsular embryonic development,

and aquatic lurval development—is consistent

throughout the genus (Martin 1965, 19674),

with the exception of the Western Australian

P, douglasi, in which oviposition is aquatic

(Main 1964), Blake's (in press) revision of

the myobatrachines includes Meracrinia

nichellsi in Psendophryne, but nothing is

known of its life history (Main 1968),

Taudactylus Straughan & Lee

Species cxamined: 7. diurnus, from ML.

Giotious, Qld.

Ovarian eggs reach 2,2 mm in diameter, but

oviposition and embryonic deyelopment are

not recorded (Straughan & Lee 1966). We

found larvae (Fig. 7B) in a slow-flowing ercek.

The anus is dextral. The mouth structure

(Fig. 6E) is unusual. The jaws are weakly

developed and there are no labial teeth; but

the disc is greatly expanded and umbrells-like,

with a complete papillary border.

The life history of ZT. aeutirostris is not

recorded, and therefore whether or not this

unique Jarval form is typical of the genus is

unknown,

wa phdh =) Dagan

meal

Fig, 7. Left lateral view of larvae of: 4. Criniz

parinsignifera; B, Taudactylus diurnus;

C, Uperoleia marmorata, In each case the

bar represents 5 mm,

42 G.

Uperoleia Gray

Species examined: U, marmoratd, U. rugosa.

Species described: U/. marmorata, from 38 km

N. of Bateman’s Bay, N.S.W.

The eggs are pigmented and have discreté

capsules; the ovidiameter is about 1.5 mm.

Development is aquatic, External gills do not

develop. The larva is unspecialized (Fig, 7C);

the anus is dextral. The mouth (Fig. 6F) has

F. WATSON and A, A. MARTIN

two upper and three lower rows of labial teeth,

and gaps in the papillary border at both front

and rear. Moore (1961) incorrectly states that

the papillae extend around the posterior mar-

gin of the mouth disc; and both Moore (1961)

and Lynch (1971) erroneously record that

there is only one upper labial tooth row.

The life history of 0. rugesa is very similar.

Life history characters are summarized in

Table 2.

TABLE 2

Life history characteristics of Australian leptodacrylid genera

Unoper Labia! Gaps in Labial

Egg Mass Development FEatretnal Gills Tooth Rows Papillac

bal

Genus Species 3 Z é = & & 38

Genus Species z= & = 3 Fa E a “4 € =

= a 7 ta w @ = + foe

a = g EN a 5 0 z 2 i=] P< Begs

e zg #4 FF = & > Z << <¢%e

ANELOTUS a ee a=, & ae

LHCHRIODUS + j= -«— oo —-— — + a» JF c=

LIMNODYNASTES ce => r= ~ > —— Le os | — t —

KYARRANLS + = — a ca — + — — + —

PHILORIA ‘ao oe f Eo ie

HELELOPORUS al Ses + = —> ~~ + —F 3 f

MIXOPHYES — + tS fd om @& = 3 «he

NEOBATRACHUS — _ + = = = = = as = =

NOTADEN — & ‘tp 2 ~s =& 4 = ==

CYCLORANA — -b + — 2 — + — —, 7 —

ASSA - ? — y 5 -

CRINIA veoreiana — oo + = 2 = — 77 — le, +:

haswelli — = = = & = 4- = = 4 =_—

faeyis — = t. — — a — + >. — +

itenif = + = + — => _ — No papillae

slenifera sroup — + — — — =

GLAUERTIA a” oe ; = -7 i. = pea

MYOBATRACHUS 2 fen > + >

PSEUDOPHRYNE ~ + 4 a = = = + — — Ea +

TAUDACTYLUS ? oat > nS] = 2 SE

UPEROLEIA >» te br a ae ia | i TS Sion —& 23

Discussion

(i) Status of tHe subfamilies

Life history data support the division of the

Australian leptodactylids into the two sub-

families currently recognized. The Myobat-

rachinae are a close-knit, natural group of

genera sharing several life history features,

These are: eggs with discrete cupsules, ege

masses not foamv; no external gills; « dextral

anus; two upper and three lower rows of labial

ieeth; and anterior and posterior gaps in the

papillary border. The few exceptions are

species of Assa, Crinia and Taudactylus whose

larvae are modified for development in a

parental pouch, or in other specialized niches.

The Cycloraninae are a more heterogeneous

assemblage. Leaving aside C}clorana (which is

discussed. below), there is still a variety of

#Th brood pouch of male

developmental patterns und larval forms in this

group. The frothy egg mass has apparently

evolved at least twice, in view of the occur-

ence of two different methods of foam produc-

tion, In Adelotus, Kyarranus, Lechriodus, Lim-

nodynastes and Philoria the foam is formed

by the female “paddling” with her forelimbs,

which have specialized flanges on one or more

fingers, during amplexus. This paddling causes

a stream of bubbles to pass backward beneath

her body and become entrapped in the mucus

which accompanies extrusion of the eggs (Mar-

tin 1967a). Heleioporuys females Jack these

flanges, and in this genus the foam is. presum-

ably produced by a different (but presently

unknown) method (Martin 1970). Again ex-

cluding Cyclorana, life history features com-

mon to most cycloranines are: eggs with dis-

crete capsules, sametimes in foamy masses!

AUSTRALIAN LEPTODACTYLID FROGS 33

external gills present, 3-6 upper rows of labial

tecth; and no posterior gap in the papillary

border. The anus is usually median, but is

often slighily offset tn Neebdarrachus, and fully

dextral in Adeloms and Mixophyes,

Lynch’s (1971) division of the Cycloran-

inae into tribes is based on breeding biology

and the position of the vomerine teeth. The

Limnodynastini consists of the genera in which

foamy egg masses are produced with the aid

of the Hanged fingers of the female. This group

is of course relatively homogeneous in terms

of life history, since if was partly defined in

this way. The Cycloranini, an the other hand,

exhibit a variety of life history patterns, and

from this point of view do not appear Lo con-

stitute # natural group

(ii) The bearing of life history data on generic

delimitation

The current generic delimitation of Austra-

lian lJeptoductylids is broadly consistent with

what is known of their life histories. In cases

where genera haye very similar life histories,

ea. Neobarrachis and Notaden, Pseudophryne

and the Crinia laevis group, there is sufficient

differentiation in adult morphology and ecolozy

tO warrant generic separation, The retnoval of

Crinia darlingtoni to Assa by Tyler (1972b)

and the subdivision of the remainder of Crinig

by Blake {in press) are supported by life his-

lory evidence. The developmental bialogy of

Assa is unique among Australian leptodacty-

lids, and the Crinia laeviy and C. signifera

groups ure also definable in terms of life his-

tory. The two members of the C. haswellf

group have rather different life history patterns,

but both are distinct from those of the C€-

laevis and ©, signifera groups,

Kyarranus and Philoria are the only genera

whose status seems questionable in the light

of life history data, The similarity between

theny in Most aspects of both adult and Jarval

morphology and ecalogy has already heen

commented on by Littlejohn (19636) and

Braitstrom (1970), and the latter has indi-

cated his intention to synonymise Kyurranus

with Piiloria. Such u change is clearly sup-

ported hy evidence From their life histones,

(ili) The position of Cyclorana

Tyler’s (1972a) contention that Cyclorane

does net cunform with the currently accepted

concept of the Cycloraninas, and has hylid

affinities, is strongly supported by life history

data. Indecd, If regarded solely in lenms of life

history, Cvclorana coincides very clusely with

the pattern typical of Australian bylids ( Martin

& Watson 1971). Characters which it shares

with them, and which are almost unique among

Australian leptodactylids, are the indistinct

egg capsules, the general body form of the

tadpole (particularly the acuminate tajl}, and

the presence of two upper tabial tooth rows

combined with the occurrence of papillae along

the posterior margin of the mouth dise. Data

from other sources, ¢.g, karyotype and mating

cull structure, ure needed hefore a final

decision can be made; but for the present it

shoukl be recognized that the subfamilial dis-

position of Cyclorana and the definition of the

Cycloraninae require revision.

liv) Phylogeny ef the Australian lepioducty-

lids

The phylogenetic relationships of the Aus-

tralian leptodactylids are disputed, Parker

(1940) speculates that the myobatrachines may

have been derived from ihe cycloranines:

whereas Tyler (1972a) regards the myobat-

rachines as the primitive, and the cycloranines

as the denved, group. Lynch (1971) believes

that the two groups are not closely related, aud

that they represent independent descendants

from a primitive leptodactyloid stock,

Our data do not contribute significantly to

resolution of this question. If Cyclorana is left

out of consideration then there are three main

distinguishing features in. the fe histories of

the two subfarnilies. These are (1) the absence

of external gills in the myobatrachines, and

their presence in nearly all cycloranines; (2)

the presence of two upper labial tooth rows in

the myobatrachines, and of three or more in

the cycloranines; and (3) the pap in the lower

labial papillae of the myobatrachines. The

latter two characters stiggest that the

myobatrachines are the more primitive group,

but not necessarily that the cycloranines were

derived From them. The presence of only two

upper labial tooth rows is common in many

families of anurans, ¢,g, most hylids. bufunids

and Neotropical leptodactylids (OQuellman

1970; Martin & Watson 1971; Lynch 1971),

The papillary gap is also a bufonid character-

istic. Thug Lynch's (1971) suggestion that the

myobatrachines may be a relatively unmodi-

fied derivative of the proto-bufonid stock (i.e,

the leptodactyloid group which was ancestral

to the bufonids) seems reasonable, Bufonids

do, however, possess external gills, Life his-

tory data do not assist in the |nterpretation al

cycloranine phylogeny, In terms of life history

characters alone the only conclusions iat can

44 G. F. WATSON and A. A, MARTIN

Key to Genera of Australian Leptodactylid

Laryae

(excluding Glauertia, Myobatrachus)

1. Larvae in brood pouch of adult male -

1. Larvae not im brood pouch of adult Miytniadtardtiaeta:

2, Mouth without labial teeth or papillae... — — — 6. ee

vtssa

.. Crinia laevis group (part)

2. Mouth with labial teeth and/or papillae oj... ee ee

Wa aA

. Labial teeth present .

4, Larvae whpiemented; freesuittatoniath i in 2 gtrearits Mt. ‘Glorious # are, + Old.

4. Larvae unpigmented or lightly pigmented

5. Larvae in pools or damp sphagnum,

pherson Range, Qld.

6. Papillac camptetély surrptinding mouth .

6. Papillary border incomplete .... me

7. Papillary border with an anterior gap

7. Papillary border with both anterior and posterior gaps .

8. Mouth with 2/2 labial tooth rows .

8. Mouth with moré than 2/2 labial tooth TOWS ccc ccecee ere cveeene Mh,

9, Mouth with 2/3 labial tooth rows! .....,.

9 Mouth with more than 2/3 labial tooth TOWS ooccce sescceescssuesiusvessesvvecnviveee Oedeomcoeece

10. Mouth with 3/3 labial tooth rows 2.000.006 ee ee ee

10, Mouth with 4-6/3 labial tooth rows _.

. Anus dextral

12, Mouth with 3/3 labial tooth rows —.......-.0...-— ~~

12. Mouth with 2/3 labial tooth rows? —

Labial teeth absent — | occsesisicsrspteerern etree

1. Anus median or neat-median pred aide

Talay dliurnas

Ris wrist pyTeronegs eel orice tetrocti tute HSE 10000 .. 5

5. Larvae in pools or damp sphagnum; Mt. Baw Baw, Vic, . ~~

or in Hepronipas in earth;

gies Philoria

Point / Lookout, NS.W,; Mac-

; Kyarranus

pes ene Teorhrevrtenetritae! pied ite daeenkirenalaiiattrs Mixophyes

Cyclorana

~ Holeioporus

Lechriodus

Limnodynastes

Es Adclotus

.. Neobatrachus

Notaden

. Crinia georviana

_. Pseudophryne

Crinia laevis graup (part)

Crinia signifera group

Uperoleia

1 Tadpoles of nearly all Australian Hylidae whose larvae are known also key out in this category.

> Tadpoles of Bufo marinuy also key out in this category.

be drawn are that the cycloramnes afte a more

specialized and less homogeneous group than

the myobatrachines, and do not show any close

affinities with them.

The phylogenetic position of Cyclerana can-

not yet be decided. In terms of life history: it

shows greatest affinity with the hylids, less with

the. myobatrachines, and virtually none with

the cycloranines. It is conceivable that it rep-

resents a relict of a primitive stock which was

ancestral, to both leptodactylids and hylids.

M. J. Tyler (pers. comm,) is currently cogaged

in an snulysis of the affinities of Cyclorana,

and until his work ts completed further specu-

lation is not warranted.

(v) Larval characters as an wid to diagnosis

The larval morphology and biology of most

genera of Australian leptodactylids are

sufficiently distinctive to enuble generic diag-

nosis to be made in terms of these characteris-

tics; they form the basis of the following dicho-

tomous key.

Acknowledgements

Much of the material used in this paper

was collected during field studies supported by

grants from the Nufiicld Foundation and the

Australian Research Grants Committee (Grant

No. 66/16172) to Dr. M.. J, Littlejohn, and by

the University of Melbourne Research Alloca-

tion to the Department of Zoology.

For donating material of species not repre-

sented in our collection we thank Mr. J. M,

de Bavay, Dr. M. J. Littlejohn, Dr. B.S. Low

and Mr. M. J. Tyler.

Some of the illustrations were prepared by

Miss L. M. Howard and Miss M. Leahy,

Dr, M. J. Littlejohn and Mr. M. J, Tyler

read and criticized the manuscript.

AUSTRALIAN LEPTOBACTYLID FROGS 45

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STUDIES ON THE ECOLOGY OF THE AGAMID LIZARD

AMPHIBOLURUS MACULOSUS (MITCHELL)

BY F. J. MITCHELL*

Summary

MITCHELL, F. J., 1973. Studies on the Ecology of the Agamid Lizard Amphibolurus maculosus

(Mitchell). Trans. R. Soc. S. Aust., 97 (1) , 47-76, 28th February, 1973.

Amphibolurus maculosus (Mitchell), the Lake Eyre Dragon, is restricted to arid salinas in the

northern part of South Australia. The lizards live near the margins of the salinas where a suitable

burrow area of fine, wind-blown sand underlies the buckled salt crust. Their essential refuge from

the harsh environment is in the permanently damp sediments, which occur below these dry aeolian

deposits underlying the salt crust.

Preliminary laboratory experiments suggest that this lizard has a high temperature tolerance

(CTM 48.9°C) and low evaporative water losses (1.1 mg/g/hr at 37.5°C)

The harvest ant, Melophorus sp., which occurs in the same habitat, is an important food item for the

lizards, and the elevated rims of the ant nests provide shade and basking sites.

Seasonal emergence, following 3-4 months of hibernation, begins when ground temperature reaches

about 19°C. At this temperature the lizards head-bask, emerging fully from the burrow when body

temperature is raised to about 22°C. Under these conditions the dominant males emerge and

establish territories in mid-August.

Basking postures are adopted to raise body temperature to 37.5°C (eccritic temperature determined

in laboratory tests). In the field, behavioural thermoregulation maintains body temperature at about

39°C during higher air temperatures. If temperature cannot be held down within this range, the

lizard retreats to the humid Jayer below the dry sand in the burrow zone.

Within the population, dominant, sub-dominant and subservient males can be recognised by

behaviour and coloration during the breeding season (September to December). Among the females,

two breeding groups, related to time of hatching, occur. Sperm retention is evident in one of these

groups, in which ovulation occurs about 2 months after fertilization.

Sexual dimorphism in relation to colour pattern is not thought to be the basis of sex recognition

since colour changes occur in both male and female. It seems likely that acute perception of size

difference is the basis of sex recognition.

STUDIES ON THE ECOLOGY OF THE AGAMID LIZARD

AMPHIBOLURUS MACULOSUS (MITCHELL)

by F. J. MircHi.i*

Summary

Mrrcuece, F. J.. 1973. Studies on the Ecology of the Agamia Lizard A.nphiholurus maculosas

(Mitchell). Trans. R. Sov. S$. Aust., 97 (1), 47-76, 28th February, 1973.

Amphibolarits maculasus (Mitchell), the Lake Eyre Dragon, is restricted to arid salinas

in the northern part of South Australia. The lizards live near the margins of the salinas

where a suitable burrow area of fine, wind-blown sand underlies the buckled sali crust.

Their essential refuge from the harsh environment is in the permanently damp sediments

which occur below these dry aeolian deposits underlying the salt crust.

Preliminary laboratory experiments suggest that this lizard has a high temperature

tolerance (CTM 48.9°C) and low evaporative water losses (1.1 mg/g/hr at 37.5"C).

The harvest ant. Melophorus sp., which occurs in the same habitat, is an important food

item for the lizards, and the elevated rims of the ani nests provide shade and basking sites.

Seasonal einergence.follawing 3-4 months of hibernation, begins when ground temperature

reaches about 19°C. At this temperature the lizards head-bask, emerging fully from the

burrow when body temperature is raised to about 22°C. Under these conditions the daminant

males emerge and establish territories in mid-August.

Basking postures are adopted to raise body temperature to 37.5°C Ceccritic temperature

determined in laboratory tests). In the field, behavioural thermoregulation maintains body

temperature at about 39°C during higher air temperalures.. If temperature cannot be held

down within this range, the lizard retreats to the humid layer below the dry sand in the

burrow zone,

Within the population, dominant, sub-dominant and subservient males can he recognised

by behaviour and coloration during the breeding season (September to December). Among

the females, two breeding groups, related to time of hatching, occur. Spetm retention is

evident in one of these groups, in which ovulation occurs about 2 months after fertilization.

Sexual dimorphism in relation to colour pattern is. not thaught to be the basis of sex

recognition since colour changes occur in both male and female. Ut seems likely that acute

perception of size difference is the basis of sex recognition,

CONTENTS

1. Introduction 2.00 2 ee AB (2) Humidity -_ [eee = Cao

4 . 49 (3) Salinity Po «te» no 256

4 Pea ane Metnede ace 7 ag 4. Food and Predation . an L 54

(2) Laboratory data... .. 30 7. Flooding of the Habitat... 58

3. Morphology of Amphibotyrus maculosus 50 8. Activity patterns and Thetmoregutatian 5k

4. Habitat and Distribution a 50 9. Survival in the Preferred Habitat — 4f

The habitat of the Lake Eyre population Tolerance to temperature and water slress 6/1)

a ane peant s 3 10. Establishtnent tnd Defence of Teericory

é burrow zone ..,, Sete ate oth the a Sra be, 62

(3) The “wet” salt zone... .., -. 51 4 A

The Lake Callabonna population... ... $1 11. Reproductive Behaviour ee

The Lake Torrens population - .. 52 12. Sex Recognition ... .., 65

Bbyesal panier OF Fie Sasa ie oa 32 13. Growth Rate and Reproductive “Cycle ff

5. Microclimate of the Hubitat ._ 53 !4 Acknowledgements =... 67

(1) Temperature, to oes ae 653) OSL References cor “Erte cto By. See tue “EG

*Late of the South Australian Museum. This paper was compiled from the late F. J. Mitchell's

draft manuscripts and ficld and laboratory notes by Ann Mitchell (Department of Botany, University

of Adelaide. S. Aust. 5001).

4h FE. 3. METCHEL1.

1. Introducton

Araphibolurus maculovas is a highly adapted

lizard, restricted in distribution to the salinas

of the Lake Byre Basin in the north of South

Australia, It was first collected in 1929 by

C. T. Madigan, who lodged with the South

Australian Museum 20 specimens taken at

the southern end of Lake Eyre Nerth in the

area now known as Madigan Gulf. These ear-

less lizards were identified as a variety of

Tympanoeryplis lineata by H. M. Hale, then

Director of the South Australian Museum [in

Madigan 1930). In a revision of Tynpanocryp-

tis, a genus of “earless” dragons, Mitchell

(1948) described the lizard as a new species,

T. maculosa.

Subsequent ostcological studies (Mitchell

1965) showed that the uffinities of this species

lie with the genus Amphibolurus and that it

represents an extreme speciulization within the

venus. The enclosure of the t¥mpanic mem-

brane, which had. led to its assignment to

lympanocrypis, was cansidered likely to be

i secondarily developed Characteristic, This

may be an evolutionary adaptation to burraw-

Ing in dry sand, and may have arisen on more

than one occasion in agamid lizards.

Lake Eyre, occupying an atea of 93500 km,

is the largest of several extensive salinas in the

arid. north of South Australia (Fig. 1), lying

aL the ‘southernmost and lowest end (14 m

below sea level) of the Lake Eyre Basin, This

Basin lies within the 125 mm isohyet in the

driest area of the Australian continent. The

usually dry river systems draining towards

Lake Eyre serve a catchment area of over

1,300,000 kn*. Some of this catchmenr lies

within areas of comparatively heavy und

regular rainfall but only under particular cir-

cumstances does sufficient water reach Lake

Evre to fill the Lake. Following exceptionally

heavy summer rains in western Queensland in

March 1949 and March 1950, Lake Lyre by

September 1950 had filled with water for the

first Lime in living memory. Scientific surveys,

sponsored by the Royal Geographical Society

of Australia (South Australian Branch) and

led by C, W, Bonython, were carried out until

the Lake had again dried out by November

1952 (Bonythan 1955, 1956, L960}.

During this period the lizard was again

observed and collected. [ts ability to spend

long periods foraging on the oper surface of

the salt crust of the Lake, withstanding both

predation und desiccation, aroused oonsiderahle

interest,

In 1964, Donald Campbell successfully

uttempted a land speed record on the surface

of Lake Eyre, In order to gain access to the

solid salt crust, a Causeway was constricted

from the shore-line across the maryinal zone

where the salt crust is thin. The track to the

causeway permits vehicular access to the shore-

line, and the causeway itself, projecting west

from Prescott Point at the tip of Sulphur

Peninsula (Figs. 1, 6), has subsequently

served as a natural “trap” and developed a

population of these hezards suitable for

behavioural studies in their natural environ-

ment. A study area was sett up at the cause-

way, where meteorological observations and

records of hehavioural responses of 2 marked

population of the livardy were made during

visits between February [965 and October

1968.

This. paper iy bused lurgely on field obserya-

tions of the lizard an Like Eyre, together with

briefer studics uf populations on other inland

salitas. These field observations were sup-

potled by vivarium studies at the South Aus-

tralian Muscum, Preliminary experimental

work is reported bnefly.

2. Materials and Methods

(1) Field? Studies

The ecological simplicity of the habitae and

the lack of a predjtor sense itt A. macnlosus

make it an attractive animal for study once

problems of distance, inaccessibility and try-

int werking condilions ate accepted. The

lizards are very alert and hecause of cryptic

coloration almost impossible ta detect except

during their sudden, rapid movements to main-

tain a few metres distance from un approach-

ing observer. During the breeding season,

however, territorial challenges, fighting and

mating continue uninhibited’ by close-range

observation.

Early in the field studies some 10 km of

shoreline were surveyed, but later observations

were resiticled to the causeway population

und all meteorological records reported here

were taken in that area.

In all, L6 trips were made lo the study area

during the period February 1965 to October

1968, Average time spent at the study atea on

these trips Was 7 days. In addition, during

September and October 1967, an extended

survey Was made of the major salinas extend-

ing in an are around the northern end of the

Flinders Ranges. regurded us potentially suit-

able habitats for the Hzards,

ECOLOGY OF AMPHIBOLURUS MACULOSUS 4g

Field data have been derived from several

sources. Continuous temperature records of air

and sand at various depths were obtained using

an EILCO thermistorised twelve-outlet, twin

channel. recording thermometer, while single

readings were taken with a Thermophil elec-

tronic thermometer. Rectal temperatures were

obtained with a Schultheis, quick-reading

mercury thermometer, All instruments were

checked and calibrated in the laboratory before

each trip. Relative humidity was variously

measured with cobalt thiocyanate papers,

Fig.

lithium chloride cell equipment and = whirling

psychrometer.

Behavioural data were obtained from direct

observation and from the marking and re-

Capture of specimens in the causeway popula-

tion, at Prescott Point. Quadrats were marked

out along the edges of the causeway and move-

ments of lizards in relation to these areas were

recorded during the period of study. Lizards

were permanently marked by toe-clipping, and

colour-coded For rapid identification of marked

specimens in the field.

LAKE la

CALLABONNAT=3 *

1. Map showing the major salinas of northern South Australia and the known distribution of

Amphiholurus maculosus. Inset map (upper left) shows portion of Madigan Gulf (the type

logality), and the location of the causeway at Prescott Point which was fhe main study area. A

hlack square indicates areas in which populations’ of A. maculasus have been observed; a white

square indicates arcas where survey of the salina margins revealed no specimens of A_ macn-

losis.

Sh F. J.

(2) Labonuery dare

Experiments on thermal criteria and tem-

perature ltolerunce of A. maculosus were

caried out in an oven preheated to 45°C.

Regular lemperuture increments of 1°C were

made at § minute intervals

Rates of water lass were derived from e¢x-

periments carried out in a thermostatically

controlled, Wauter-jacketed incubator under

temperature conditions controlled to =0,5°C.

‘Yhe test chamber wus also desiccated over

silica gel to ensure a relative humidity of less

than 4% at all temperatures.

Experiments to deterntine water loss through

the integument were undertaken with the vent

of the animal sealed with waterproof adhesive

lupe amd the head inserted through a_ thin

rubber membrane across the mouth of a con-

tainer partly filled wath silica gel to absorh

avy Water lost through the ittegument. The

silica gel was overlain hy u piece of thin card

on which the lizard’s body restect.

The test animals were acclimated for at

least seven days to coriditions involving the

daily allainment of their maximum voluntary

activity temperature (39.8°C), Animals were

tested hetween 1000 and (500 hours during

their period of maximuin activity.

For long-term behavioural studies, a ter-

rarium was set up which successtully simulated

lake shore conditions. A layer of gypseous

clay. maintained in moist condition, was aver-

lain by 15 cm of drv sand from the lake

shore, Over fhe sand, pieces of consolidated

salt crust provided a surface similar to the

burrow zone area.

Both light and heating were provided by

au battery. of high-power incandescent lamps

mounted under an adjustable hood. ‘Time

switches controlled day length, and the posi-

tion of the hood controlled the maximum

temperature, Strong correlation between field

observations and laboratory tecords was Found

for daily and seasonal activity cycles and the

onser of reproductive activities.

3, Morphology of Amphibolurus macplosus

Amphibolurus maculesus shows several

features OF morphology, physiology and be-

haviour Which reftect its adaptation to arid

silinas, Its dorsal surface is white to very

pale grey with u row of very dense black

blotches on either side of the vertehral line,

Dorsally and laterally there are smaller black

and rusty-hrown pigmented areas, This colour

MITCHELL

pattern gives excellent cryptic coluyralion on

the salt surface, the dark areas blending with

the shadows of small holes and pinnacks on

the rough salt (Figs. 9, 10, 15). The ventral

wurfuce is white with a dark streak cxtending

longitudinally along the centre of the throat

to the gular fold, Colour variations related to

the environment, ani the striking colour pat-

terns developed during the breeding season

will be discussed later in this paper.

The adult male attains a total length of

about L1.5 cm (snout-vent length 7 cm}, the

adult female being smaller ut about 10.0 cm

(snout-vent length 6 cm).

The eye ts small and deeply sunken and is

protected from salt glare by promiment ser-

rated eyelids with dark pigmented Jinings

(Fig. 4), The nostrils, while showing a circular

external opening, open inte the nasal cavity by

only a narrow slit, directed forward and down-

ward, This structure prevents the nasal pas-

sages from becoming blocked when the lizard

burruws through joose sand. Speci! nasal

stwucture has been described by Stebbins

(1943) in the Americun venus U/ma, which is

a sand-burrowing form. He has shown (Steb-

bins 1948) that other American iguanil

genera including Uru, Helbroakia and

Phrynesonea, all of which habitually burrow

in loose sand. have similarly adapted nasal

structure.

4, Habitat and Distribution

The type locality of 4. meaculasies 1s Madi-

gan Gulf, Lake Eyre North, out from the

mouth of the Frome River. The species is

widely distributed around the southern shore-

line of Lake Eyre North and around the

nerthern ind south-evstern shorelines af Lake

Eyre South. Throughout the study every oppor-

tunity was taken ta search other lakes for

additional populations and practically all of

the major salinasy in che State were at Jeast

cursorily cxamined for signs of habitation by

these lizards. Two additional populations

were found: uw population in the saline areas

at the southern end of Lake Callabonna and

extending soulhwards through the salt chan-

nels inte the northern tip of Lake Frome, and

nother population along the north-western

shoreline of Lake Torrens, Fig. 1 shows the

area searched, the localities from which speci-

mens have been taken, and the range over

which this species is known to occur.

The geomorphology and the history of land-

forms In the Lake Eyre Busin have been dis-

cussed by Wopfner & Twidale (1967). Evi-

ECOLOGY OF AMPINBOLERUS MACULOSUS 3|

dence from fossil deposits suggest that exten-

sive areas Of brackish water or saline swamps

existed Within the basin from mid-Tertiary to

the end of the Pleistocene. The ongin of the

salt in Lake Eyre has. been subject to debate

but i stems likely that both cyclic sult and

connate salt, accumulated from waters brought

inte the basin from the extensive drainage

system, have contributed (Bonython 19546;

Wopiner & Twidale 1967; Twidule 1968),

The present isolated populations of A, mracy-

fases, which although spatially widely sepa-

rated ure virtually morphologicylly — indis-

tinguishable from ane another, may be relict

from uw more widespread species evolved in

association with the shoredines of the Sarge

brackish lnkes and swamps that were a feature

of the Lake Eyre Basin during Pleistocene and

early Recent periods.

THE HABITAT OF THE LAKE EYRE

POPULATION

The habitat within the study area can be

divided into three distinct zones, the “beach”.

the “burrow zone” and the “wet salt zone”

(Fig. 5). This zonation can be readily identi-

fred throughout the distribution of the Lake

Eyre population examined, bit is much less

distinct in the area of ibe other two poepttly-

tions.

1. The beach; tn tie area along the southern

shoreline of Lake Eyre North which was

most intensively studied, the beuch is backed

by near-white sandhills varying from low

consolidated hummocks stabilised by low

shrobby vegetution { Nitraria, Seaevola) to high

drifting dunes encrouching upon the lake. In

Many arcas low cliffs varying in height from

about a metre to upproaimately 12 m above

the lake hed expose Recent to Cretaccous sedi-

ments to face the lake Continuous wind

erosion transports large quantities of gypsi-

ferous clay and grit and other aeolian fines

out over the beach and on to the surface af

the lake, The beach is usually a narrow strip

of consolidated sand Frequently intermixed

with wreas of very coarse sand and pebbles.

In areas where it is not overlain by recent

drift it remains damp during the cooler months.

Typical pebble beaches occur in some areas

and the height and form of some of these

beaches suggest sustained periods of strong

wave action in the very recent past,

2, The burrow zone. This term has been

adopted to cover the zone tn which most of

the activity of the lizards takes place. It con-

sists Of un trea of distomed, dry, crusty sur-

face, varying From a few metres wide (im areas

where flooding upproaches close inshore or

where little pypsiferous drift is brought out by

the prevailing wind) to 400-500 m wide in

stidom-flooded embayments where wind-

drifled deposits have accumulated on the sur-

face (Fig. 5), This 5-15 em thick layer of

fine gypsiferous clay and sand rapidly dries

out and in doing so cxpands and distorts the

Salty crust which Sorms over the top of i.

In section, this provides a burrowing substrate

consisting of an irregular, salt-impregnated.

crust up to 2 em thick, lying aboye approxi-

mately 10 em of fine, dry, windblown sedi

ments underlain by sand which is kept con-

tinvally dump from the water-table 40-70 em

below,

The lizards break through the salty crust at

a weak point and then literally “swim” through

the fine mobile scdiments below until they

encounter the high humidity associated with

the damp consolidated sand at lower levels.

They remain there until their re-emergence js

triggered hy rising temperatures or some

internal stimulus.. They follow the thermal

gradient hack to the surface, frequently

emerging at a different point to that of entry,

3. The “wet" salt zone: The solid salt crust of

the lake varies from about 2 cm in thickness

in inshore areas to about 40 cm in thickiess

fowards the centre of Madigun Gulf. This

crust, overlying wet gypseous clay. becomes

distorted and buckled as the salt recrystallises

on drying out (Figs, 7, $). Although most of

the activity of this lizard takes place within

250 in of the shore, both the lizards and the

nesta of the ant Melopkorus sp. (their princi-

pal item of food) have been observed more

than 1400 m from the shore linc, During the

territorial season, many young subordinate

mules are forced to live outside the burrow

sone and are frequently found well offshore.

While liltle weight can be placed on the salt

surface without bringing water to the surface,

the actual surface “skin” js dry most of the

lime except in cerlain effiorescent areas close

to shore which are continually damp. Relative

humidity readings using cobalt thiocyanate

papers set | cm off the salt under a shield.

gave readings as high as 55% over these

efflorescent areas, bul in other areas the read-

ing was below 15% and equalled the reading

at 100 cm above the surface.

THE LAKE CALLABONNA POPULATION

Essentially the same conditions prevail as at

Lake Eyre. with the lizards living around the

52 Fr. J. MITCHELL.

southern margins of the lake on isolated

patches of aeolian drift in association with dry

saline crust, A suitable habitat is not present

in northern parts of the lake, where fresh

water from the Strzelecki Creek has leached

the bulk of the soditim ancl catefum salts from

the surface deposits and the water table is

deeper hecause of extensive Recent lacustrine

deposits on the surfuce.

THE LAKE TORRENS POPULATION

The surface of Lake Torrens is wet and

muddy und the take frequently contains water.

As a consequence the population has adjusted

its behaviout to living amung low vegetation

along the immediate shoreline and upon jow-

relieY islands covered with chenupodiaceous

shiulbs.

PHYSICAL FEATURES OF THE BURROW

ZONE

Field and laboratory observations suggest

that there are three essential habitat charac-

teristics Which influence the cistribution of

this lizard,

|, A surface crust: Specimens placed in a

laboratory cage containing either loose sand ur

consolidated sand lacking a surface crust were

upable ta burrow, ‘They were only able to

scoop oul a shallow depression, Several ficld

observations related to this were made during

the 1952 flooding of the lake when most of

the lizards were forced onto the damp beach.

Some did succeed in finding crusted areas back

among the veyetation but several lizards were

found im shallow depressions against drift-

wood wong the beach. Presumably the sur-

fave crust is casential in providing initial pur-

chase against which these lizards start their

“swimming” procedure in burrowing through

the sand, Vhe consolidated surface crust need

no. Hecessarily be saline and in fuct, gypsiferous

sediments hus Logether by filamentous blue-

green algae may well have provided a suitable

hafritat surface over wide areas in the past

and may prove io be aw contributitig factor at

present.

2, A layer of fine dry sand (and/or clay) about

10 em thlek under the erust: In order to pro-

vide adequate insulation from the extreme

heat of the summer, the fine sand or sand«

yypsiferous clay mixture must be dry and

about 10. em thick. It is probably important

that the sediments contain pypsum to promote

expansion and rapid drying after wetting.

3. A constant source of humidity Jor Me re-

treat: Because of the water balance problems

inherent in living upon a salt surface sub-

ject to exlrerne lemperature, mw is essential

that the environment provide a refuge in which

both evaporalive und respiratory water Josses

be minimised during the periods of retirement

underground. The sediments al about I) cm

helow the surface crust must be permanently

damp,

PRESENT KNOWN DISTRIBUTION

At most of the localities examined along

the shore of Lake Eyre North and Lake Fyre

South, lizards for “signs of their presence)

were observed whenever a combingtion of the

three factors described above were found. This

applied equally well to Lake Callabonna ex-

cept that suitable habitat there is much more

limited. Most of the northern part of Lake

Callabonna and Lakes Blanche and Gregory

have uo very friable surface deposit of fine

gvpsiferous clay which is not bound hy a

surface crust. This is not a suitable habitat.

Lake Torrens lies on the “weather” sie of

the Flinders Ranges and is therefore subject to

more frequent flooding than the other lakes

around the northern end of these ranges. The

lake surface is therefore permanently wet and

does not provide a suitable habitat, but at the

northern end and particularly along the western

side, suitable conditions occur along the actual

shoreline and upon Jow insular greas where

the pale gypsiferous clay supports sparse

halophytic vegetation, Many of these arens dry

out during the warmer months, and form a

suitable habitat with a distinct surface crust

underlain by varying depths of dry pale yellow

to red gypsiferous clayey silt, This habitat i

exploited by the Lake Torrens population,

Specimens have been collected up to 275

metres back into the vegetated zone away

from the margin of the lake,

Chher Jakes examined were Lake Harris,

Lake Gairdner, Lake Everard jind Lake Hart

(Fig. 1). Although knowledge of the shore-

line conditions gained during this survey was

very fragmentary, the yeneral information

gathered is considered adequate lo suggest

that if any additional populations are found

on any of these lakes, they will not be found

living upon the surface of the lakes as at Lakes

Eyre and Callabonns, but along the margins

as at Lake Torrens. The sufface conditions

of these Lakes ure similar to Lake Torrens,

the surface being too wet le support the ants

ECOLOGY OF AMPHIBOLURUS MACULOSUS 52

(Melophorus sp.) which provide the principal

item of diet for these lizards; these ants, or

other species of similar burrowing habit, are

restricted (a the shore-line areas. In many of

the Jakes, the ecological situation occupied by

the unis ut Lake Eyre is taken over by 4

species of Fighting Spider (Geolycosa sp.).

Cicindeline beetles are also frequent and active

predators over these damp lakes and in part

Teplace the ams as surface scavengers, They

dig vertical burrews into the damp muddy

surface an@ huve only been seen ut the Lake

Eyre stiidy area when layers of fresh silt from

fioodjags were overlying the salt:

5. Microclimate of the Habitat

A. macilosus has a strict preference for the

Taargins of the salinas and does not invade

the white sandhills despite ts competitive

daminunce., in cage experiments, over the

only agamit species which occurs there

(Amphibolurus pictus Pevers), It was noted

also that 4. pictus makes burrows over a

metre Jong and up to 20 cm deep in mid-

summer, despite the fact that its thermal

tolerances are only slightly inferior ta those of

A, maculosus (see Table 2), This suggested

that the lake surface environment may have

some thermal advantage over the adjacent

sandhills, Climatic conditions prevailing within

the habitat were studied in an effort to deter-

mine the reason for the strict habitak prefer-

ence and also to provide a foundation for an

analysis of the activity and behavioural pat-

terms observed,

(1) Temperature

Using the thermistorised recording ther-

mometer, aa allempt was made to compare

the temperature profiles of the sections. of

the burrow zone preferred as a refuge by

the lizards with parallel situations in the

adjacent sandhills. Comparison between sum-

mer (February) and winter (July) temper-

alure patterns for both the burrow zone area

and the nearby white sand-dune area js given

in Fig. 2. Summer soil temperature profiles

for burrow zone and sand-dunes aré shown

in Fig. 3, The data obtained proved difficult

to evaluate, probably because of the difficulty

of obtaining strictly comparable test. sites, The

ground humidity varies from place to place

with the local soil structure conditions and

the thickness of the surface drift, and the

extent to which the ground water has pene-

trated towards the stirface also varies. It is

nut possible to assess these fuctors without

breaking the surface crust and thereby dis-

turbing the stratification of the protective

layers winder which the lizards normally rest.

Therefore, while the lizards were found con-

aistently to prefer to rest on or just in the

damp sand underlying the mobile dry sand,

it Was seldom possible to determine wher

the tip of the thermisior probe was lying in

this same position. Aljso the protective value

of the surface soil was greally reduced by

local #ain which increased its conductivity, All

of these factors reduce the comparative value

of the data.

"The data, however, do allow iwo conclusions

to be drawn with reasonuble confidence.

Firstly, during the cooler weather when both

the burraw zone deposits and the adjacent

sandhills are damp to the surface, the thermal

characteristics are essentially the same. Second.

ly, in midsummer the temperature at average

refige depth (10 cm) in the burow zone,

probably due to the thermal capacity of

the water table 40-70 em below, is lower

und subject to less fluctatlon (30=1,5"C)

than the temperature in an equivalent situation

in the adjacent sandhills (34%4°C) (Figs.

2, 3).

{2) Humidity

Surface temperatures were recorded using

a contact thermistor and a Thermephil elec-

tronic thermometer. Because of the salurution

of the lake floor right to the surface and the

periodic appearance of free water on the sur-

face of the more thickly salt encrusted area,

it was anticipated that evaporative cooling

would contribute to lowering sutface temper-

ature of the Jake and raising humidity, particu-

larly at the “living level" of the lizards (1 cm),

both being features which would improve its

suitability, as a habitat during the warmer

months. However, careful testing with the

thermistor probe revealed the acttial surface

of the “wet” salt to be dry and at the same

temperature as the crust in the burrow zone

and ue sand in the sandhills. Similarly, tests

with cobalt thiocyanate humidity papers at

1 cm and 100 em above the lake surface

and 100 em above the adjacent sandhill sur-

face usually gave the same treading, Over the

temperature range 30 to 40°C, during which

lizards coukl he expected to be active over the

“wet” salt surface, the readings were usually

below the minimum sensitivity of the paper,

mdicating relative humidities below 15%.

a4 F. J. METCHELL

Humidity teadings, derived from each af

the sources described ubove, varied from Jess

than 5% to 55% refative humidity. ‘The

higher readings invariably followed light rain

or thundery conditions and were the same

for sandhills and lake surface sites, As air

lemperuture increases each day, over the solid

salt crust, the “wet” salt begins to “sweat”

und brine appears at the tips of small, self-

sealing, salt pinnacles. Due to the high tem-

peratures and high evapurative rate it ts likely

that. any humidifying effect of this brine is

restricted to a microtayer, of perhaps only

a few mm, just above the evaporative sur-

face, However, tf was not possible to detect

higher humidity over the “wet” salt surface

and this is possibly due to inadequate instru-

mentation,

13) Saléstey

The salinity: of the wind-blown silts deposi-

ted in the burrow zone varies with depth.

Salts dissulved out from the superficial layers

were 7-11% of the silt; 3-5 em down, 4-8%

and 5-10 em down, 3-4%. Below this level

the salinity steadily increases again up lo

saturation at the water table 40-70 cm below

the surfate, The decrease in salinity nearer

the suftface is probably due to the recent

ofigity of the surface deposit and to condensa-

tion dlong the line of demarcation between

the permanently dampened sands and the

overlying dry sediments leaching the salt out

over a period of time. The lizard} normally

rest in this zone of lower salinity but whether

this is of any advantage is: unknown. The

sand along the foreshore also contdins 2-4%

salt and the observed salinity stratification may

he due to an increuse in surface salinity hy

wind drift from the sandhills rather than to

desalination of the intermedinte luyers.

Several small areas of white efflorescent

salts were found just outside the burraw zone

and these areas are continually Josing water

la the atmosphere, Although no. hzards were

ever ubserved using one of these areas on a

hot day. the large number of fecal pellets

Fig.

present on and around them suggest that their

thermal sdvantages may be ulilised by the

lizards. The surface temperature of such an

area of about 3 m* near the main study site

was compared with that of the surrounding

salt and found to be up to 9.5°C lower

It appeurs that the Jake surface confers no

advantages upon an inhabitent, either in terms

of surface temperature or humidity, over the

condition prevailing in the surrounding sand-

hills. Despite the abundance of free saline.

water throughout the habitat it may still be

inadequate to prevent the high evuporulive

rate [about 220 cm per annum (Bonythen

1955)] from creating sufficient dry hygroscopic

salt throughout the habitat to place greater

strain on the water balance of this species

than other desert-adapted lizards.

The permanently damp layer under the pro-

teelive crust in the burrow zone provides. a

high humidity retreat into which the hzards

ean Tetire overnight or, if under social or

environmental stress, for much longer periods

without endangering thew water balance. This

is regarded as the key factor an restricting

the species Wy the marginal urcas of the

salinas.

6. Food and Predation

The main food source for A, macilosus is

the harvest-ant, Melophorus sp. In addition

to providing food, the nest-mounds of these

wots are important “features” in the generally

featureless habitat, providing lookout points,

basking sites and the only source of shacle.

Colonies of Melophorus generally occur on

the “wet-salt” surface usually within 750 mm

from the beach zone; preference is shown for

areas where the salt-crust is no more than

2 em thick and underlain by telatively clean

sund down Lo the water-table 40-70 em below.

The colonies are regularly spaced over the

tuke surface, each being about 10 m equi-

distant from the next (Mig. 8}, Investigation

of a nest revealed a setics of upper gsuallerics

just beneath the sult crust and i single verticy!

hole z0ing down about 40 ein to a second set

2, Comparison between summer and winter thermal characteristics of the borrow zone and adja-

cent While sand dunes, Figures from continuous recorder traces of temperature were platted ut

40 minute intervals.

~ temperature at -10 em

-——--—- lomperuture at -l cm

-- +). oir temperature at 40 em above ground

4A) Burrow zone temperatures over 34 hour periods in February, 1965 and July, 1966, Tem-

Peroture range at--10 cm for the February period was 3.5°C, about a nivan of 33.6°C.

(B) Sand dune temperatures. over 34 howe perinds in March, 1965 and Tuly, 1966. Temperao-

thre range al -10 em for the March period was 1 1L.5°C. about 4 mean of 34.6°C.

ECOLOGY OF AMPHIBOLURUS MACULOSUS 55

A pe Pky

7 ead! xt teal

é ~ o

c N ¢

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| ¢ \ 7

4 LN eo

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u fy ut Re fat

é a tan

L < Le

/ —T te ee : f

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ay as mee ee ee

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E ay 22% FEBRUARY 1965 Ore cee ae an aad

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E-s Ls s woot ‘

. a Rare

R Fete

Ee - a.

oAP20 er ate f Ls

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a a

19 JULY 1964 har a 20"

é 8 10 12 14 16 18 20 22 24 2 4 6 8 10 12 14

ee ee Se ee a ee! ee ee oe es en re” jee i L =| = ! | fe D Re | homeo, |

TIME - HOURS

| 40

2°49 MARCH 1965

T “7S

U e ie

PY te

°C

23" JULY 1966 Tee ee sry Pull 2ath

HHO ys Tee

6 8 10 12 14 16 18 20 22 24 2 4 é 8 10 12 14

be L i i He ees 1 L ni Ly gt AP estoy ke L be Ves L 4

TIME - HOURS

FIG. 2

SH FJ. MITCHELL

of galleries at or slong a consolidated layer

of clay just above the water-table, The Gon-

suruction of these galleries produces, on the

surfuce, a distinctive crateriform mound up

to 2) cm ja height. The sand below the salt

crast is usually covered by a fine layer of clay

Which probably accounts for the reddish-

brown debris, brought from below, being in

marked contrast to the while salt crust,

At any time, only 9 small proportion cf

the total wumber of nests contain active

colonies, The ants show linited activity dur-

ing the day, appearing at the surface only to

deposi sand grains from the workings below

round,

In yicw of the limited aboye-surface activity

of the wnts, it has been suggested (Madigan

1930) that Melophorus baryests micro-

organisms either in the salt crust (blue-green

algal cells) or in the damp sand above the

water table (Dunalielle spp.). The nests usually,

however. contain insect remains. and the ants

have been observed gathering bodies of insects

trapped on the sult. Probably most foraging

uclivily by the ants oecurs at night.

A. niculosus, also, is an Opportunistic

feeder and when other insect life is available

on the lake surface, the lizards feed on a wide

ranve of different insect species. On most

nights numbers of insects are stranded on the

salt. surface. Their presence may be explained

in several ways, With jin, offshore wind many

insects may be blown out over the lake;

others may be attracted by the rise in humidity

over the lake surface af night; aquatic insects

(particularly on moonlit nights) may mis-

lake the white lake surtuce for walter. Overall

the Jake surface produces a vast “white sheet”

effest — un cimmmonty used form of insect

trap—and many insects are Ifapped on the

hygroscopic salt surface and killed when

temperature increases next morning, During

ihe spring months, September—November.

vast quantities af insect Jile may occasionally

be stranded on the lake surface. The bodies

of insects Which have been neither captured

by 4... mueu/osny nor later scavenged by Melo-

hig,

phorus become incorporated within the sur-

face salt layers.

it ls Of Intevest thal the characteristic insect

fauna developed in the vegetation of the shore-

line and sand-Aills is rarcly stranded on the

salt surfuce of the like, while the majority

of species stranded on the salt are seldom

seen about the shore.

The period of greatest feeding activity of

A, maculasus (February to April) frequently

coincides with drought conditlons in the sur-

rounding country, and consequent limited

supply of windborne insect life.

Tn view of the limited number of ants active

on the surface, the lizards nist lorage out

over the lake surface for long periods at high

temperatures. The lizards dig into the sides

of the ant nests to retrieve ants from inside,

and the more frequently visite ant-nests

closer tnshore become very battered in appear-

ance, Shallow depressions scraped out at the

base of the nests provide small areas of shale

intu which the lizards may retreat.

The Lake Dyre population ol A. maciulosus

displays no response to overhead predators,

relying lor safety on their cryptic coloration,

The only possible protective cover on the lake

surfuce ts provided by buckles and cracks in

the surface of the salt crust (Figs, 7, 13).

Although these would seem to provide ideal

reweuts they arc tarcly used by the lizards.

The crystalline swit in ihe erust provides a

“glasshouse” eflect and the temperature below

the ¢mist may be several degrees higher than

the surface of the salt. When pursued aver

the surtace until exhausted, the lizards are

more likely to come to rest in the shade of

like pursuer than to retreat helow the salt crust.

There is Jittle evidence of other potentiil

Predulors moving ot across the salt surface,

Hawks. constitute one Of the main predators

of A. piceus from the sandhills adjoining the

Jake. On several ovcusions dead specimens of

A. picts have been observed well off-shore

on the fluke surface. Presumubly these have

been dropped by hawks. The fact that these

3, Yautechrones (soil-air temperature profiles at. different times during the day) recorded on 6th

March, 1965 for (A) burrow zone area and (B) sand dune urea. Differing thetmal characterts-

tics of the two localitics result in the more rapid and greater heating in the sand dune area,

At—I0 cm (averave burrow depth of A. muculases) in the burrow zone there is a temperature

range from 30,9 to 35.6°C over the timc period recorded. At the same depth in the sand dune

area there is a temperatitre ratige from 31.4 to 4L,.4°C over a similar time Interval, In (B), due

to the limiled range of the thermometer used (calibrated up ia (20 F (49°C)), no figures are

avallable for (he 2 em and 4 em depths at ihe 1120 and 1515 readings. Field notes recorded

that, at these times and depths, the temperature Was “12Q°F-+> nd rising rapidly”.

ECOLOGY OF AMPHIBOLURUS MACULOSUS

4 se } ¥4

SURFACE

E |}

E 7 0630 1100 1600

25 30 35 40 45 50

— 1 1 aoa 2 —- lhe sie, ® re 1 Sy

1“. 1

TEMPERATURE ‘°C

i> Z \ \

SURFACE + - = a aa si

|} I as 5

0600 Q?30

TIaAymg

—1

pe)

10 ? 1120 1815

25 30 35 40 45 50

t . i P af t

TEMPERATURE ‘°C

FIG. 3

38 BF. J. MITCHELL

captures have not been retrieved would sug-

west that the glate From the Jake surface may

confuse werial predators.

7.. Flooding of the Habitat

The periodic flooding, either of the whole

ot Luke Eyre or, following more localised

ruins, of restricted areas, must affect both

Melophorus and A. maculasus:

Melophorus colonies withstand flooding for

consideruble periods by becoming sealed off

below the water. As water disappears from

the lake surface, the colonies soon “break

out” wand tework the galleries and nest. The

shape of the above-sutface mound would give

protection to the opening of the nest during

light flooding.

When the nurmal burrow zone is Mooded,

A. maculosus retreats to the shore line and

lives, precariously, in the sand there. The

lizards are frustrated in atlempls to retire

underground since there is no consolidated

crust. to provide Jevernge for burrowing, and

they have no refuge from predators such as

the Ground Goanna {Mararnus gouldii Gray)

ugainst which they have adequate protection

in their narmal habitat, Among the lizards

forced ashore by flooding, colour changes

occur in which the backgtound colour of the

lizard becormes a deeper grey and the areas of

black and rusty-brown pigmentition become

more numicrous and intense, giving 2

speckled appearance more similar to the pebbly

heach sands, At times of flooding, large nuim-

bers of Silver Gulls (Larus novae-hoflandine

Stephens) ure attracted to the arca and these

probably constitute the greatest predation

hazand tor A- maculovay.

An interesting response 10 flonded conditions

has been observed in A. maculosns, During

winter at fow ground temperatures (down to

16°C) the lizard is in torpor. In vivarium

experiments at low ground temperatures, (14-

16°C}, flooding of the substrate aroused lizards

which had been belew the surface in torpor

for 3-4 weeks. Emergence to the surface

involved a greater degree of muscular ¢o-

ordination than is usually shown at these

temperatures nnd may be triggered by lack of

oxygen. Inflation of the body when it emerges

from underground ensures that the lizard floats

on the surface of the water. It would appear

possible that such a reaction would assist

survival of the animal in face of encroaching

floadwatets.

Localised areas of water in the lake show

marked response to changes of direction and

velocity of wind, A flooded inshure area may,

within a few hours, appear us an exposed

sull surface anil vice versa, This dust impose

uidditional problems in the re-establishment of

both Afelapherus and A. maevloases in their

preferred habitat,

8, Activity patterns and Thermoregulation

Like other ectothermic animals, the activity

af Amplibolnvus macelesus depends on

temperature. The lizards show definite be-

havioural fesponses al cerlain temperatures

and these responses serve to keep the body

temperature within a preferred activity range.

Throughout the season of lizard activity. varta-

tions occur in the means and ranges of these

temperatures, These variations, imposed by the

uge and sex of the particular lizard and its

position in the social structure of the popula-

tion, are considered later, The basic range of

temperatures associated with various wetovities.

summatised in Table 1, fs dictissed here

During the winter months (May to Augusr)-

A. maculosasy remains in torpor helaw ground

Emergence threshold air temperature is 19°C,

at which temperature there is early season

emergence (August-September). under stress

of hunger and drive for the establishment of

terrttory, in males. Ac this temperature only

the head of the lizard is thrust through the

salt crust. It is darkly pigmented in the pineal

tegion and the eyelids are extended, indicat-

ing accumulation of blood in the cephalic

sinuses, The morphology of venous shunts in

the cephalic region, and their role in head-

hody temperature regulation, have been

described for Pkrvnetame cornutum by Heath

(1964, 1966), Although the anatomy of the

head of A. mtack/osus has not been examined,

there is similarity in head-basking hehaviour

hetween this lizard and PArynesoma, Which

is Known to use this aid to rapid stimulation

of the central nervous system and elevation

of body temperature. It seems likely that A

maculosus usts a similar mechanism. The

head-busking position is only maintained until

the body temperature is raised to 22°C, at

which temperature the body is Fully exposed

at the mouth of the burrow, Tt is at this tem-

perature that most lizards first emerge for

the season in September—October. During

early busking stages the body of the hzard

is orientated with the back cxposed to the

sun (or source of heat in the vivarium), and

the body ts inflated laterally and closely

ECOLOGY OF AMWPAIBOLURUS MACULOSUS ay

pressed to the substrate, with the hind legs

spread out flat behind the body in a “swim-

ming” position,

Under laboratory conditions, with air tem-

perature at 23°C, the adult lizards emerged,

with eyes still closed, as soon as the lights

came on. Within 10 minutes all were fully

emerged and awake in the flattened basking

position. Within 30 minutes rectal tempera-

tures had risen to 30°C at an air temperature

of 23,9°C,

During summer, mean burrow temperature

(al about 10 em depth) is 32°C. Under these

conditions daily emergence occurs with first

light, and temperature is no longer the cons

trolling factor.

The basking position is maintained until

body temperature reaches 26-27°C, when the

hzards first start to move away from the

burrow and ate sufficiently co-ordinated to

feed.

At a body temperature of 32°C, the lizards

ure capable of Cull range of movement and

activity and, in hot weather, they move out

onto the salt crust at this temperature. The

eceritic or preferred body temperature, was

determined in the laboratory by use of a saw-

tooth thermocline. Under laboratory condi-

TABLE I

dency of A, maculosus in relation te body

femtperature

| |

ee |

49,5 °C tothal temperawre uncontratud

=48.9°C—CTM f hentine

aso!

2-43" C omantenee

aA = | temorceutatory

40°C - tem neruture

—39C—oominiled Lemineraure (lod) | enntan|

AIS ervenitictonierature Cab,)

55° |

| 26¢>—nn Activity

eae

27-289 C—maye frm burriy Huskie range

ais Oe

12° C—ful emergande

19% —rarly emergence; head basking

tions the top temperature of the basking range

is 37.5°C. At this temperature there is re-

orientation of the lizard from the positive to

negative with respect to heat source,

In the Vivarium, the lizards can retreat

under-grournd at any time, whereas in the lake

habitat, they must return from the wet sali

surface ta the burrow zene to retire under-

ground, In the vivarium they retreat under-

ground at a body temperature of 37-37,5"C,

While in the field they remain active on the

salt surface away from the burrow zone with

body temperature held at about 39°C.

Except under very hot conditions, the lizards

have a normal activity cycle of about 8 hours

per day. This long period of scavenging is

correlated with food supply and is necessary

lo ensure that they obtain sufficient food. In

summer, during, much of this time air and

surface temperatures would be over 45°C. At

these temperatures the body of the lizard is

held high off the salt surface, the only points

of contact with the bot surface being the

feet and end of the tail. If stationary for any

length of time, the toes of the hind feet are

Taised from the surface so that there is con-

tact only with the limited area of the heel.

During thermoregulatory maintenance of

hody temperature at ahout 39°C, use ts made

of the diversity of substrate conditions pro-

vided by the buckled salt crust, of the small

ateas Of shade cast by the ant nests and of the

few small pieces of driftwood embedded in

the salt surface which ate used as elevated

perches,

Since, during the hotter summer months.

there is an established behavioural pattern

of daily movement out from the burrow zone

onto the “wet” salt crust as the temperature

tises, it seems likely that the lizards achieve

same thetmoregulatory advantage in this

ured.

While measurements revealed no consistent

decrease of temperature or humidity over the

“wet” salt, this may simply reflect the techni-

cal difficulty of detecting small changes on the

actual surface of the crust.

Slight pressure on the “wet” salt crust

releases moisture to the surface, accompanied

by 4 rapid, transitory fall in temperature due

to evaporative cooling (particularly when a

wind is blowing). The lizards, by scratching

at the ‘surface of the crust, may achieve this

same cooling effect for parts of the body in

contact with the surface, It is noticeable that

AD TP. J. MITORree.

during the hot months, which coincide with

the defence of territury by the dominant

mules, the young males forced to spend con-

siderable time out over the salt surface devel-

op uccumulations of salt on the digits of all

limbs (Vig. 11). There may also be salt

encrustation along the ventral surfaces of

these lizards. This sale accumulation may be

caused by the lizards seratching at the sur-

face of the salt crust in allempts to bencfic

from any slighl evaporative cooling elects.

When no longer able to control body tem-

perature by adjusting position and stance, the

lizard Must retreat fo the burrow zone and

retire underground, In order ta reach the

cooler, wet sand Jayer near the water table.

the lizard must first penetrate the Joose sand

below the salt crust, The upper layer of this

loose sond muy reach w temperature of 60°C.

A, maeulosus must have a short-term toleranee

to this extreme temperature in order to benefit

from the hwnid layer below,

Wf Foreed to remain active at higher temper-

atures, A, wraculosus begins to “pont” at a

hody temperature of 42-42.5°C. In this action

the mouth is opened wide (Fig. 10), and

there is u steady rate of deep breathing at 60

breaths/ minute. Unlike some other lizards

(ew, Varanes spp. A, pietus, A. tnermts)

there arc no associated movements of the

gular pouch during panting in A. muculosts,

Tolerance of temperatures. above 42°C, at

which thermoregulation begins to break down,

are discussed below.

Preferred body temperatures and thermo-

regulatory behaviour of several other species

of Amphiholuruy Wave been described by

Bartholomew & Tucker (1963). Bradshaw &

Main (1968), Brattstrom (1971), Heatawole

(1970), Lee & Rarham (1963). Licht, Daw-

son, Shoenwker & Main (L960), and Pranka

(1971 a. b).

9. Survival in the Preferred Habitat

‘The habitat preference of Amphibolnrus

moculosus is unique among vertebrate animals

and many factors would appear to count

against survival im such a harsh. extreme

environment, There jire obvious problems in

maintaining water balance, arising from the

hygroscopic salt surface on which the lizard

spends much of its time, compounded by lack

of aceceys to free water from which to supple-

ment its supply, and the need to handle a

higher than average sodium intake. (The ants,

Melopherus sp.. have uw high salt content

(Braysher 1972!) and many of the insects

(rapped on the lake surface huve salty encrus-

tation on their body and legs), The survival

oF an insectivorous animal in a Vegetation

free habitat, periodic flooding of the lake.

high summer lemperatures, and lack of cover

from the sun, are all matters which require

spectul physialogicul of behavioural siljust-

ment

However the liza has the ability Lo &xploil

this habjtat successfully. The low rate at

reproduction (one to four egeys per female per

anium) sugeests that its biology is more than

adequate to meet the environmental stresses.

As with all desert-adapted animals, behavioural

avoidance of environmental extremes (Schmidt-

Nielsen 1964) has been shown to be a key

factor jn survival in this harsh environment,

hut the study also indiested that the enviren-

mental stresses encountered require consider-

able physiologicul adjustment to ensure sur-

vival. The wide scape ol this study has only

permitted superficial examination of these

adaptive mechanisms. and more detailed

studies have been undertaken by other

workers,

Taleranee 1 teniperadive ane water stress

Survival of Aimphibolurus pacniosus in the

lake Eyre habilat involves ability to with-

stand high temperatures and to cope wilh the

lack of free water,

Preliminary experiments were carried oul

16 determine some of the thermal critena and

rates Of evaporative water Joss. Although the

results are based on very few reuclings, the

data are presented here since they ure the

only records available for this species, Com-

parison is made wuh published data tor two

ather species of Amphibolurus: A. pictus

Peters and A. inerinis (De Vis), Both of these

species are widely distributed in desert areas

and oecur in the sand dune country ailjacent

to Lake Eyre. A. tnermix is generally found in

red sand and A. pielus shows preference for

white sand. Comparisons between A, plac

logs, A. picmn and A inermis are summarised

in Table 2,

i Braysure, M. 1. (1972).—-Water and electrolyte balance im the agurmid ligated Amphibolurax

mocntosny. (Mitchel. and the structure and function of the nasal solt gland of the sleepy lizard,

Trachivdesanrus rugesus (Gray), Unpublished Ph.D-

Vhesis, University of Adelaide.

ECOLOGY OF AMPHIBOLURUS MACULOSUS él

TABLE 2

Thermal criteria and rates ef evuporative water loss for A, maculosus, A. pictus and A, inermis

A. maculosns : A. piewus ~ Aimermis -

Mitelich, Miicach, Warburg Mitchell, Warburk = Lichr- Rawson Bradshaw & Ueatwole Rradshaw

present study present study f1965h) present study 9nsh) & Shoemaker Main (1968) (1970) (1970)

T1966)

Eouritie sya”

termnerabune

CT™ aa,9°> a5" ase 485°C 44,550 465°C

Lethal 495°C 49.6°°

feMpPeralu re

Survival 300 min a B40 min 480 min. 103 min. hI+G.As

£59 ar4gzec at 44ec an46e°C —omtins at 46°C

EWL VAG meester 158 m2/2/hr O33 ns/sfhr 1.052 0.0913

ar37.sec at a7.s°C at arsec mem! hr

ar asec

The critical thermal maximum (CTM), de-

fincul by Cowles & Bogert (1944) as that

Temperuture at which a reptile loses nruscular

co-ordination. has heen determined for a oum-

her of Australian lizards (Warburg 1965 6;

Heatwale 1970).

Comparisons between these data are diffi-

cult to make because of differences in ex-

perimental procedures. Also, the usefulness of

this thermal criterion has been criticised

because some lizards: after losing muscular co-

ordination and passing into a coma, are cap-

uble of recovery if held at that temperature

or if the femperattre is lowered. Other lizards

do not recover after these muscular spasms

and die quickly, or within a few haurs-

The CTM for A. mectiosas was. determined

using only 5 specimens. "The test lizard was

placed in a beaker in an even maintained at

48°C. After 15 minutes the temperature was

raiscd at the rate of 1°C every 5 minutes,

The average CTM for A, inaculasas, derived

from these five test animals, is 45.9°C. Two uf

these (one male, one female) recovered fully

when the temperature was lowered after the

lest, The temperature from which there has

been no recovery after cessation of muscular

spasms. has been recognised as the lethal

temperature for this species.

The survival times at high temperaiures

have been revarded by some authors ys more

meaningful criteria) and these have been

determined for several Australian agamid

lizards (Warburg 1955 a, b: Licht, Dawson

& Shoemuker L966; Bradshaw & Main 19468).

Por A. mactlosus, a survival time of 6.5

hours at 45°C was recorded, and over this

period an 8% loss of body weight occured.

Texts curried out at 42°C resulted in death

between 22 and 25 hours following a loss of

6.3% of the hody weight

TF death yt this Jow level ef hody weight

loss Jef, 34-4996 Joss at death for some

iguanids (Hall 1922)} were due ta desiccation

only, it would indicate a rather low tolerance

to desiccation for A. macnlosus and its depen-

dence on retreat to the humid region above the

salt water-table of the Jake. Further evidence of

low desiccation tolerance bas been observed in

the vivattum where deaths occurred when the

artificial “water-table” was not muintained and

sub-surface humidity level dropped.

Evaporative water losses haye been deter-

mined for 2 number of Australian lizards

(Warhure 1965 a,b, 1946; Dawson ef al,

1966: Bradshaw 1970). Attempts to measure

evaporative water losses of 4. niaculosus were

carried our using test animals either fresh from

the field or which had been acclimated to a

24 hour evele involving the attainment of tem-

peratures in excess of their maximum voluntary

activity temperature. Animals were tested be-

tween 1000 and 1500 hours, their most active

part of the day.

The five animals tested yaried from 8 g ta

14.5 2 in weight (mean 10.5 g), Although the

meusured EWE, rate for A. yaculosux varied,

probubly in relation to the degree of activity

of the test animal, the average value was 1,10

me/e/hre (08-1.5 meg/erhr). Of this total

EWL, pulmonary losses contributed 0,83

me/e/hr (0.52=1.15) and 0.27 me/e/hr

(0.42-0.29) was due to cutaneous loss,

Bradshaw (1970) has found significantly

lower cutaneous and pulmonary walter loss in

the desert-adapted .4. mermis than in other

species of Amphibelurus from more lemperate

habitats, His results suggest that the improved

water economy of the desert-living specics ix

due both to reduction in the metabolic rate

and to alterations in the integument.

In Table 3 comparison is mide between

cutancous and pulmonary water [oss in A.

maculoses and A. inermis.

The Jaw propertion of total EWL attribu-

table to cutaneous loss in the present figures

62 F J. MITCHELL

for A, muculosus suggests that the integument

may be further modified against evaporative

losses.

More detailed work is required to accurately

define the critical ambient and body tempera.

tures, and rates and sites of evaporative loss,

in A. maculosux. However, available data do

TABLE 3

Rates of eittineous and pulmonary water lossy in

A. maculosus and A. inermis

A. maculosus A inermis

iT 5 6

hody Weight 10.5g 24.1+0.97¢

total RWL 1.10 mg/g/he 1.05£0.0913

mg/g/hr

cltaneous 0.27 mg/g/hr 0.452-0.0933

mg/g/hr

pulmonary 0.83 mg/g/hr 0.57=0,0778

mg/e/hr

c/P ).33 0.80

suggest that its Lemmperalure tolerance is among

the highest known for Australian lizards, and

that evaporslive Water Josses are among the

Jowest recorded,

In its natural habiuu, A, ntaculosas, like

other heliothermic reptiles, uses a series of be-

havioural postures and movements to maintain

body temperature within a preferred activity

range. This activity range of ftetnperature is

higher in the field than the eccritic or preferred

temperature selected by the Jizards in a labora-

tory temperature gradient. However, except

under some conditions imposed by the social

hierarchy, the lizards can avoid intolerable heat

levels by retreat to the damp sand of the bur-

row zone, Subservient mules, kept away from

the burrow zone by the dominant tales, are

forced to spend long hours on the salt surface

with a consequent high level of body heat.

Survival under these conditions must indicate

the existence of plrysiological capacities to

withstand high temperature and to restrict

water loss, High body temperature is tolerated

passively and water is conserved by lack of

evaporative cooling mechanisms.

10. Establishment ond Defence of Territory by

the Male,

The early emergence, in tute August, of

dominant males of the previous season 1%

usually preceded by these lizards positioning

themselves just below the salt crust where they

can more quickly respond ta imcréasing tem-

peralures. By mid-September the territories

established by these dominant males are under

challenge by the younger males which have

subsequently emerged. An old mule challenged

and displaced by a young male retreats under-

ground for the remainder of the breeding sca-

son (September to late December). By mid-

October the tertitorial situation has become

fairly stable, and remains so throughout the

breeding season.

Apart trom the juveniles (siout-vent length

<40 mim), three categories of male can be

recognised in the dominance hierarchy,

(1) Dominant: lizards which exhibit display

behaviour and fight and never retreat from

another male. These lizards develop

marked breeding coloration with bright

orange-yellow ventro-latcral murkings

grading to brilliant. reddish-orunge ven-

trally with « pale patch mid-ventrally. The

reddish-orgnge murkings extend onta the

base of the tail and under the thighs.

Sub-dominanit: lizards which exhibit dis-

play behaviour and which retreat instantly

from a dominant mule but will fight to a

decision among themselves. Among these

lizards a “peck order” is established des-

(2)

pite their individual territories. These

lizards alsn develop good — breeding

coloration.

Sufservient males: lizatds which do not

exhibit display behaviour, and) which re-

treat from all other males or rol] over

into. submissive posture on their backs if

attacked, Only very faint yellow ventre-

fateral eMlours ure developed by these

lizards.

The territorial defence of the dominant

males follows a classical pattern. Each tetri-

tory is centred upon a look-out site, usually a

amufl mound of salt 10-20 cm above the sur-

ronnding salt, or a piece of sull-encrusted urifi-

wood embedded in the lakc, The area of

territories varies about un average of 15 m

radius and is, in part, dependent on the virility

of the controlling mule. Orientation within their

own territory and that adjacent to it fs, at

least partly, by sight and the boundary between

the tennitory of two dominant males is known

ta those two males lo an accuracy of a metre

ar so. ‘The forcing of one mile over the

boundary immediately precipitates att approach

and challenge from the adjacent male, This

technique can be used to determine hierarchy

patterns in the ficld in arcas where terrilories

af dominant males are adjacent, Male TH will

ECOLOGY OF AMPHISGLURUS MACULOSUS a

flee if forced onto the territory of male I, but

will fight (and win) against male Lin bis home

territory,

The display behaviour of the dominant

males invalves a typical push-up movement in

which the forelimbs ate flexed and the whole

of the forepart of the body moves. A short

frog-like leap is followed by two quick push-

ups. In challenging another male. the gular

pouch is lowered and full threat display

follows in which the body is raised high and

compressed laterally $0 as to increase apparent

size by enlarging the profile during a lateral

confrontation (Fig. 12). This alsa displays

fully the bright ventro-lateral markings.

Usuully the mouth ts opened wide (Fig. 13).

This display is usually adequate to deter in-

truders [rom entering the territory. When male

to male fighting does occur an established pat-

terh of events is observed. There is long-range

recornitean and challenge at distances of up to

4m. then the commanding dominant closes

the distance until a counter challenge is issued

ata distance of about 3 m, after which the two

males approach each other to a distance of

about 0.5 m. There follows up to 10 minutes

of bluff behaviour, side stepping, continual

facing-up and counter-facing in an effort ta

get the tai] into position to lash the oppanent’s

head and forelimbs, and the head in a position

where it is possible to bite the opponent’s hind

legs and buck of the tail (Fig. 13). Head-on

encounters also uccur with the opponents’

jaws becoming interlocked in tenacious biting

In an cleven minute encounter, the langest

ohserved, between males T and I ia the hier

archy, three physical clashes occurred. The

biting was directed at the hind limbs and each

clash was Over in an instant, the attacker being

flung vetticully by the momentum of the

tunge and the evasive endeavour of the

opponent,

There may be overlap in the territories estab-

lished by the sub-dominant males. While the

dominaats remain “on guard” in their terri-

tory throughour most ot the day, the sub-

dominant males adjust their emergence times

so that only one ts active within the territoty

at one time.

Subservient males adjust their emergence

limes to periods when they are less likely to

be pursued by the dominant males—in the

heat of the day or late in the afternoon. Their

level of tension in the presence of the dominant

male is reflected in their respiration rate which

may be as high as 120 breaths/ minute as com-

pared with 35 breaths/minute for the domin-

aint. They spend a very limited amount of time

on the surface and then avoid recognition by

flattening themselves, with head down, against

the sult and remaining motionless for long

periods. It challenged they immediately turn

Over onto their backs in submissive posture.

Once ground temperature excecds the

threshold the dominant males will emerge at

about the same time (10 minutes) each morn-

ing independent of light intensity oF

temperulure, Heath (1962) records a similur

temperature and light-independent emergence

in Phrynosante, suggesting the presence of

endogenous circadian rhythm. During the

breeding season this emergence lime gels

carlicr by about 30 minutes each month. Aftce

the breeding season emergence becomes rcan-

dom and the dominant males generally spend

more time underground, At thes time there is

an increase in acuvity of the subservient males

which spend longer periods active on the sur-

face of the lake, There is a lowering of ten-

sion between dominants and subservients (re-

flected in the fact that respiration rates are

simitar for both), and the subservients are Jess

inclined to retreat underground or to remain

“froze and thereby inconspicuous for Tong

periods, Territorality is not actively enforced

after the end of December and, while the

dominant male spends considerable periods

underground, the subservient males embark on

an active period ef feeding which involves

frequent excursions out over the lake tn search

of the unis which, at this fime of year. con-

stitute the main food item. In the absence of

the dominants, the subservient males may

establish territories between existing territorial

areas.

The dominant males show a renewed burst

ol activity in early April, presumably feeding

intensively before retiting underground, The

dominant males and Jute developing females

extend their activity period into May, whereas

all others retire into terpor during about the

third week of April.

The dominant males and the juveniles are

the first to emerge and last to retire both

daily and annually. Under vivarium conditions,

with temperature muintained at 27°C for 12

months, the dominant males and juveniles re-

mated active throughout the 12 months. The

subservient and sub-dominant mules and the

females went into normal torpor despite the

maintenance of temperature, These lizards

emerged for 1-3 hours every 16-30 days. The

64 bE, J. MITWHELL

reason for these arousals from torper ts not

known.

In the confined conditions of the vivarium,

the dominance hierarchy of the “population”

is establishecl within about an hour. Hierar-

chicul structure can be readily determined by

observation of respiratory rutey which range

from 30 breaths/ minute in the dominant male

to 120 breaths’ minute in the subservient males.

Carpenter et al, (1970) have described the

display and aggression behaviour of three

species of Amphibolurus (A. barbatus, A.

retlewlarnys inermis and A. murtcais) aod com-

ment on the close similarity between the dis-

play patterns of these agamic lizards and the

Jeuanidae which haye been more Fully studied

(Carpenter 1967). The display action patterns

uppear to he sbecies-specific both in the

Ignanidae and the Agamidae, The display pat-

tenis of A. miaculosus haye not been fully

analysed hue the same range of postural

changes, ivolving head and forelimbs, des

cribed by Carpenter ef al. (1970) have been

observed. Brattstrom (1971) discusses the

range of postures associaied with social and

(thermoregulatory behaviour in A. farhatus.

11, Reproductive Behaviour

Vhe adult females of Astphibolurus

mutculosus do not emerge until some weeks

after the dominant males have established their

lerritories. First to emerge at 21"-23°C in mid-

Seplember are the older females, followed,

through to mid-October, by the younger

females. The females establish burrows around

the margin of the dominant male territories

and do not, at this time, move far from the

burrows. A small group of six to-eight burrows,

all within a metre or so of one another, usually

indicates the presence of a female. At this

time of year the burrows are frequently Te-

occupied and enlarged whereas later, in the

hotter weather, « burrow is seldom used twice.

During the first week or so after cmergence

the females are pot ready for mating, and

adopt two methods to repel the advances of

a male. ‘he ficst of these is circumduction, All

females of reproductive xize (>45 mm) cir-

cumduct with either forelimb in the presence

of a male, and the rate of circumduction 1s

accelerated if they are approached by the male

or come inty competition with the male for

food (Fig, 14), Secondly, should circumduc-

tion fail as a deterrent, the female twists over

on her back and lies immobile. Both these

manoeuvres serve to distract the male hy des-

troying the “female image” to which he has

responded,

Most muting activity, and much of the terri-

torial fighting, takes place at 34°-36°C, several

tlegrees below the temperature (39°C) at

which dhe body is maintained by thermerceu-

latory behaviour. Consequently during the

mating season {October to Deceniher) greatest

activity occurs between 0900 ond 1100 hours,

While feeding and terjtorial defence take

place at 39°C, preoccupation with thermo-

Tegulation prevents sexual activiry.

The male upprouch to the female usually

begins with the male elevating his head to

maximum height in order to confirm identifica-

tion of sex. He then undertakes a series of

energetic head-bobs, followed by one or two

“frog-leaps” during his rapid approach to the

fernale. A receptive female turns slowly from

the oncoming mule und wails to be overtaken.

The male approaches the female directly from

behind and with his jaws grasps her by a fold

of skin just behind the occipital region. Using

this nape grasp, the male rolls the female

over On her side. With the tail of the male

under the tail of the lemale, the cloacae lie

¢lose Logether and a hemipenis is inserted, The

pair remain rolled on their sides for the dura-

tion of copulation (about 25 seconds) with

the body of the female arched hack with fore-

limbs clear of the ground (Fig. 15}.

Folluwing copulation, the female usually

lick in a subservient position, with the head

flat on the salt, for 15-20 seconds before

moving. During this time the male “frog-leaps”

away. Females undertake weak head-nodding

during the breeding season, invalving a simple

dip and rise of the head, The exact purpose of

this is unknown bul, in view of the cryptic

coloration, it may possibly serve to muke

known their presence ta other lizatds.

Following ovulation and ferlilization, 2

number of changes occur in the appearance

and behaviour of the females. In u fertilized

fernale, ventro-lateral coloration changes fram

pearly-white to i bright orange-red, the edges

of the lower jaw become orange, and there

develop two orange patches between the fore-

limbs and two elongate orange patches along

the flanks. Also ciccumduction ceases, and

more efficient defensive behaviour ia adopted.

Upon the approach. of a male, confrontation

lakes place with the female raising the head

as high as possible and swivelling it around

to prevent the male from getting over or past

ECOLOGY OF AUPHIKOLURUS MACULOSUS 5

her If this fails, or if the male’s approach is

so fapld that this blulE is unlikely ta succeed,

the: female rolls over onto her back, frequently

well before the male makes physical contact

with fer (Fig. 16). Distracted by the changed

image the male ustially withdraws several feet,

with some head-bobbing. After 15-20 seconds

the female vighty herself, inflates the gular

pouch and stomach, wnd compresses the bady

to display the orange ventro-lateral surfaces

and so present the largest possible profile to

the inale, The female then adopts a still-legged

attitude Which hfts the body clear of the suh-

strate and with slow, deliberate steps advances

straight towards the mule. She usually passes

close in front of him, often forcing him to

withdraw a few steps or to transfer his body

back on to the hind limbs, lifting the front part

of the body to allow the femule to pass close

under his snout, After passing the male, the

female continues to walk with the stifflegped

gait, stopping on each rise in the salt crust

to look back at the male over her shoulder.

When qhout 6 m away, her pace quickens and

finally she relaxes and runs at high speed over

the salt lo disappear behind « fold of the salt

crust.

Io contrast to their timidity early mm the sea-

son, femules, once fertilized, become quite

aggressive and will attack a male should he

compete for food at close quarters. While

carrying developing eggs the female emerges at

the same time as the dominant niales and

spends maximum possible time in basking pos-

tures. Perhaps the orange ventro-lyteral

coloration of the female at this time increases

heat absorption from the substrate. Ventral

colour change in the gravid fernale has been

reported in the American lizard Crotaphytusr

collaris by Fitch (1956) and in Callisanrivs,

Copt:oseurus and Holbyookia by Clarke

(1965).

Evvs are laid 20-25 davs after fertilization,

The female digs a distinctive burrow for egg-

laying. Normally these lizards merely nose

their way under the salt crust and “swim” at a

shallow angle through the fine, dry drift sund,

down to the damp consolidated substratum.

The ¢ge-laying fernale carefully selects a site,

usually along the shore-line, of consolidated

sand dainp right to the surface. This egedaying

burrow is steeply angled (about 45°), extend-

ing down 21-25 em, with a distinct chamber

at the bottom in which the eggs are deposited.

Young females Jay only 2 eggs while older

ferales produce 3 or 4, After deposition of

the eggs the entrance to the burrow fs filled in

again, Observations, both in the ficld and in

the laboratory, Sugeest that each fernale digs

and fills several egg-laying burrows before she

finally deposits the eggs, Whether abandon-

ment of these early burrows is due to distur.

bance ov whether there is careful sclection of

sume particular set of conditions, is not known-

The salt content of the shore-line sund is 4-5%

and this, apparently, does not impede develop-

ment of the eggs. Attempts to hatch eggs

under laboratory conditions indicate that

maintenance of fairly high humidity during

egg development is important. Fenvales fre-

quently cmerge from egg-laying in poor con-

dition and highly desiccated (Fig, 17). The

ventro-lateral colouring fades from orange to

yellow to white after deposition of the eggs.

Hatching occurs after about 70 days and

the hatchlings (SV length 25-30 mm) first

appear in January and conlinue to emerge

uatil April.

12. Sex Recognition

Jn most animals showing marked sexual

dichromatizm it ts the male which is more

brightly coloured or stronely marked. On this

basis il was accepted, in early stages of this

study, that large specimens of Amphihelurus

maculosus with bright yellow-orange-red ventro-

lateral surfaces were male and that this

brilliant colouring was a key factor in the sig-

nal pattern of male to male sex recognition

in territorial behaviour. The sex of tagged

lizards was recorded on this basis of presence

or absence of ventrolateral coloration,

Recapture of marked specimens revealed

two stages of development at which colour

changes confused this simple interpretation.

Firstly, there is the change from pseudo-female

to male colour and behaviour at the time the

mate reaches the size of an adult female, In

some cases, specimens showing weak male

coloration were observed to show the usual

female responses of circumduction and tonic

immobility. On dissection, lizards of this group

(all within 43-38 mm SV length). proved. to

be male. Recapture records revealed that, up

fo S58 mm SV length, the first-year males of

A. maculasits show the yellowish ventrolateral

markings typical of the female after egg-laying.

Lizards of this size (up to adult female size)

and coloration are repeatedly identified as fe-

male by the dominant males and are driven

oul to the margins of the colony by Lhe re-

peated unwanted advances of the males, This

ob FP, 3. MITCHELL

suggests u possible dispersal mechanism within

the population,

Secondly, some lizards which had been

mitially tecorded as female, on subsequent re-

capture showed hrilhant ventro-lateral color-

ing. Allied with change of colour, there was a

change in behaviour with these lizards now

counter-challenging an approaching male. This

change from nearly-white female to brilliant

orange psevdo-male coloration and the change

in defensive behaviour and aggression follow-

ing ovulation and fertilization have been des-

eribed previously.

While sexual dichromatism exists, ubserya-

lions Auggest that coloration has little if any-

thing to do with sex recognition in A-

macntosuy, The female undergoes considerable

change in intensity of coloration Erom com-

plete luck of ventroJtateral coloration through

pale yellow to brilliant orange afler miiting,

but. is pursued by the dominant males at all

stapes in the development of this colour pat-

tern,

A first-yeal’ male. on the other hand, may

show typicul male colouring, with prominent

rusty spols oa the shoulders and weak gular

pouch stripe and yet be repetedly mistaken

for a female, Thus, first-year males, whether

they have developed mule coloration or not,

are recognised as female within the first-yeor

female size ringe of 46-58 mm.

In an effort to determine the role played by

colour in sex recognition, and to determine

whiul colour pattern might act as an innate re-

leasing mechanism in territorial display,

domimant males in the vivarium were presented

with « range of coloured models, sintulating

male colorution. None of these elicited any

response other than an investigatory lick.

The above observations suggest size lo be

the basic factor involved in sex recognition and

suggest that size judgement is particularly goud,

In relation to clevation (most look-out sites

in the habitat of the lizards arc no more than

20 em ubove the Jake surface), A. meaculosus

shows remarkubly acute vision, Observatians

of territorial challenges in the fieldt have indi-

cated that these lizards have perception of

movement and recognition of posturing at dis-

tances of 50 metres.

Both laboratory and fiel! observations indi-

cple That there is some individual recognition

between members of the line hierarchy ¢stab-:

lishvd in the vivarium and between males of

adjvining (erritories in the field population,

TABLE 4

Relationship af size fo uge in Amphiboluruas

muaculosus

Mean SV length of A.

maéulostix (mm )

Female Male

Isl year 438 54

2nd year 59 64

3rd year fl 67

4th year 62 70

This significance of size ond accuracy of

size perception would also be a u key factor in

the effecuveness of the bluff behaviour, Unless

the lizards had such an appreciation of size and

ils Significance, the act of increasing the wren

to view by enlarging the lateral profile would

not be effective asa bluff deterrent.

13. Growth Rute and Reproductive Cycle

Over the periad of study, 376 body

measurements (SV length and tail length)

were recorded for marked and Unmarked speci-

mens.

Based on field recapture of marked speci-

mens and vivarium specimens for which age

histories were known, niean SY lengths of

Amphiboluras maculosus in relation lo uge wre

shown in Table 4. The figures represent the

mean maximum measurement recorded at the

end of the active season for cach year. Mean

SV length of hatchlings is 30 mm, It seems

likely that A. maculosny dies wt the end of the

third breeding season, at 3-34 years, No older

specimens have been recovered among the

marked population at Lake Eyre,

When adult mules emerge at the beginning

of the season in September, the testes ate Fully

expanded (9x 5 mm). Smear tests show active

spermutogenesis trom September through to

mid-December and active sperm have been

found in the vas deferens in Octoher, Novem-

ber and December, In tate Wecember there is

a rapid contraction in size of the testes to

6 x 3 mm. No uctive sperm have been found

in testes or epididymes from January Lo April.

This decline in male fertility coincides with

the onset of the period of reduced activity in

the males. Between late December and curly

March the older miles spend only short

periods on the Jake surface and Jonger periods

underground, At this time, young mules move

back into the territorial areca, subservient miles

emerge for lonyer periods and they and the

fomales, exhausted after egg-laying. embark

on tong hours of feeding, There is litde terri-

tori] defence, Ihe dominant males unly weakly

ECOLOGY OF AMPFUIBOLURUS MACULOSUS

Dominant Mate

TABLE 5

Summary of reproductive cycles in Amphiholurus maculosus

First yr, male First yr. Firs: yr amt a “Adult

female UA) female «R) Female

testes

defending (with a slight lowering of the gular

pouch) a small area immediately around their

burrow site.

The older males show a more active feeding

period through mid-March and April. During

this time the testes, together with abdominal

fat bodies, expand rapidly prior to the onset

of hibernation.

Information from recapture of tagged speci-

mens, as well as laboratory observations, indi-

cates that among the first-year fernales of the

population there is a bimodal pattern of ovula-

tion,

Females hatched during January-February

ovulate in November-December. A second

series of females, hatching Jate in April, ovu-

late in February, Both these groups of females

show maturity (as evidenced by ovulation) at

10 months. Of these 10 months, at least 4

winter months (May, June, July and August)

are spent in torpor. In the earlier part of the

active breeding period (October to Decemiber)

the dominant males mate with the adult fe-

males. Towards the end of the breeding period

the 1st-year females, down to 46 mm SV

lengths, are successfully mated by the dominant

males,

Sperm retention in the female 1s indicated by

the decline of male fertility in December and

Januars inactive | _ [

a’exien Hatching Ovulation Acilve feeding

February Inactive j

March Active feecdine Hatching tee

April Active feeding it?

Testes and far 5 Hatching

huadivs expatica '

May

June . i

Hibernalion |

July | Hibernation | Hibernation | Hibernation f Hibernation

August First

emergence’ H

Sentember Establishment of |

territory,

Spermatogenesis ; : A

4 ka / Ovulation

Octaber Spermutngencsis Tdentified as Marine

Mating with sdilt feinale, Retreats Cotour

females [to edge of terri- change to

. | torial uric pseudo-male

November Sprermutogenesis

Mating with adult | Ovulation

fetnales J nt

. 7 i aune

December Soenmatoxcncsis Returns ta Mating Euetaviag

Mating with Tet territorial

year females, _ area

Contraction of Exe-Jayine

the fact that ovulation in the late-hatched fe-

males, which had been mated in December,

does not acur until February. In March these

females lay eggs which hatch in April.

The males hatched in January and February

are sub-adult (with female coloration and be-

haviour) in November-December. Table 45

summarises male and female reproductive

cycles of A. maculosus.

Acknowledgements

The author of this paper would have wished

to acknowledge many instances of assistance

and helpful discussion during this study.

Thanks are due fo a number of colleagues who

pave assistance during the field trips, and to

the late Elliott Price and the families at

Muloorina for their help and hospitality on

many occasions. The assistance of Miss Carol

Pulley with long-term laboratory observations

and records is gratefully acknowledged. Miss

Pulley’s careful organisation of the available

notes and records of this work has made the

present compilation possible. The compiler is

extremely grateful to her for this. Thanks are

due also to Mr, Michael Tyler and Dr.

Michael Smyth for helpful comments on the

manuscript.

Fig.

Fig.’

Fig.

13.

14,

45.

16.

17.

F.. J, MITCHELL

CAPTIONS TO FIGURES 4-17

. Amphiboaluruy maculosus, showing detail of the head with deeply sunken eye, visor-like eyelid,

and absence of visible tympanic membrane.

Margin of Lake Eyre, looking north towards Prescott Point at the tip of Sulphur Peninsula,

Instruments recording continuous air and sub-surface temperatures are set up in the burrow

zone area. The beach is backed by low white sand dunes and to the left the thin distorted

crust of the burrow zone merges into the thicker, smoother salt crust of the “wet” salt zone.

. View back along the causeway towards Prescott Point (October, 1966), Quadrats were set up

along this causeway and movements of tagged lizards were recorded in the area over several

years.

- Buckled surface of salt crust on Lake Eyre. View towards Prescott Point.

. Nesis of the ant. Melophoruy sp., are regularly spaced throngh the “wet” salt zone. The

above-surface mounds of these nests are visible here as dark spots (from their shadows) in

contrast to the white salt surface.

. A. maculosus male against the disturbed base of Mclophorus nest-mound. These mounds are

used for basking and shelter and as vantage points by the lizards.

. A maculosus, overheated by pursuil, showing panting reaction typical at raised body tempera-

tures. Note deep “lens-hood” protection for the eyes.

. Salt clods on digils of a forelimb.

- Dominant male in full threat display. Body raised and laterally compressed, gular pouch and

stomach inflated.

Dominant males fighting. Specimen in background shows compressed and raised body, gular

pouch lowered, and mouth open for biting. The tails are brought into play to whiplash the head

and forelimbs of the opponent. (Dark areas at base of tail are identification marks, )

Circumduction by A. maculosus female,

A maculosus in copulation. The male biting and holding the female by skin fold behind the

head,

A maculosus female (left) showing post-fertilization colour development on lower jaw (the

under abdomen is also bright orange) and the typical defensive position. relative to the male

on the right.

Female, after egg-laying, showing lateral skin flaps under conditions of starvation and dehydra-

lion,

ECOLOGY OF AMPHIBOLURUS MACULOSUS 69

AMPHIBOLURUS MACULOSUS

ECOLOGY

MITCHELI

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~ fu 2 se, :

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ECOLOGY

OF AMPHIBOLURUS MACULOSUS

74 Fk. Lo MITCHELL!

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ECOLOGY OF AMPHIBOLURUS MACULOSUS 7s

74 FE,

I MITCHELL

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Pranks, F, RB. (1971a)—-Comparative ceology of

two lizards, Cupeia S97) (4), 129-138,

Pranks, E, BR. (1971b).—Ecology of the apanid

Nizar lnplibalures isolepis in Western Aus-

tralia. Copeia 197) (4), 327-536.

SCHMIDT-NIELSEN. Ke (1964). Desert animals:

physiological problems of heat und water,

(Clarendon Press: Oxford.)

Srnpuins, R. C. (1943), Adaptations in the nusal

pussages for sand burrowing in the saurnan

genus Clma, Am. Nat. 77, 38-52.

Sreppins, RC. (1948).--Nusal structure if

lizards with reference to olfuction and condi-

tioning of the inspired air, Am. J, Anal, 83,

[83-22 1.

Twinare. ©, R., (1968).

(Nelson; Melbourne. )

Wanpurc. M, R. (1965a)—The influence of ame

hient temperature and humidity on the body

lemperatire and water loss trom two Aus-

tralian lizards. Tiliqua ragasé (Gray) CSein-

cidae) and Avmphibeluruy bartiafity Cuvier

(Agamiduel. daner J. Zool, §3, 331-350.

Warsuro, M. R. (1965b)—Studies on the en-

vironmental physiology af some Austrian

lizards from arid and semi-arid habitats, Aust

J. Zawl. 13, 363-975,

Wagauira, M. R. (1966).—On the water economy

of several Australian geckos. ugiumds wud

skinks. Copel 1966 (2). 230-245,

Worener. Ho & Twinacr. ©, R. (1967) -Geo-

morphological history of the Lake Fyre

Basin. Jn J, N. Jennings & J. AJ Mabbutn

Eds... “Landforny studies from Australia and

Now Guinea”. GA,N.U. Press; Canberra }

“Geomorphology”.

VOL. 97, PART 2

TRANSACTIONS OF THE

31 MAY, 1973

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Rutland, R. W. R. A note on Major Structures in the Willyama Complex -

Preiss, W. V. The Systematics of South Australian Precambrian and Cam-

brian Stromatolites. Part II - - = = = a

Maconochie, J. R. Studies on some species of Hakea (Proteaceae) - - -

Kleeman, A. W., & Milnes, A. R. Phosphorian Lavendulan from Dome Rock

Mine, South Australia - - = = & A ~

Lee, D. C. Rhodacaridae (Acari: Mesostigmata) from near Adelaide,

Australia. If Ecology - - - - - ~ - “

903/

127

135

139

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

A NOTE ON MAJOR STRUCTURES IN THE WILLYAMA COMPLEX

BY R. W. R. RUTLAND*

Summary

RUTLAND, R. W. R. (19731.- A note on major structures in the Willyama Complex. Trans. R.

SOC. S. Aust. 97(2), 77-90, 31 May, 1973.

The schistosity in the transect studied forms divergent fans about the axial planes of one major,

upright, open synform which covers the greater part of the area, and a complementary antiform in

the east. This suggests a genetic relationship between the schistosity and the major structure

although the schistosity is not strictly congruous to the synform, since bedding tends to show a

dextral relation to schistosity in both limbs.

Minor folds with approximately axial plane schistosity (Group One folds), lineations, and

schistosity-layering intersections do not show a simple relation to the major folds but exhibit a wide

variation in plunge in a NNE trending zone corresponding to the dominant attitude of the

schistosity. Group One folds tend to have northerly plunges in the east of the area in the hinge and

east limb of the Mt. Vulcan Antiform, and south-easterly plunges in the west of the area in the west

limb of the Parnell Synform. The intervening shared limb of the two structures shows variable

plunges from moderate northerly in the east through reclined to southerly. The schistosity-layering

intersections show a much wider variation in any one sub-area than the Group One folds. Group

Two folds which fold the schistosity show a closer correlation with the schistosity-layering

intersection which may therefore control their orientation.

The complexity of this pattern is apparently related to an important earlier major deformation

episode, which produced major isoclinal folds. Schistosity sub-parallel to layering in the limbs of

the major structures may belong to this earlier episode.

A NOTE ON MASOR STRUCTURES IN THE WILLYAMA COMPLEX

by R. W. R. RutTLAnp*

Summary

JkuTLAND, R. W. R, (1973).—A note on major structures in the Willyama Complex. Trans-

R. Soc. .S. Aust. 97(2), 77-90, 31 May, 1973,

The schistosity in the transect studied forms divergent fans about the axial planes of one

major, upright, open synform which covers the greater part of the area, and a complementary

antiform in the east. This suggests a genetic relationship between the schistositv and the major

structure although the schistosity is not strictly congruous to the synform. since bedding tends

to show a dextral relation to schistosity m both limbs.

Minor folds with approximately axial plane schistosity (Group One folds), lneations,

und schistosity-layering intersections do not show a simple relation to the major folds but

exhibit a wide variation in plunge in «a NNE trending zone corresponding to the dominant

altitude of the schistosily, Group One folds tend to have northerly plunges in the east of the

area in the hinge and east limb of the Mt. Vulcan Antiform, and south-easterly plunges in the

west of the area in the west limb of the Parnell Synform. The imteryening shared limb of the

lwo structures shows variable plunges from moderate northerly in the east through reclined

to southerly. The schistosity-lavering intersections show a much wider variation in any one

sub-area than the Group One folds. Group Two folds which fold the schistosity show a

closer correlation with the schistosity-layering intersection which may therefore control their

orentation.

The complexity of this pattern is apparently related to an important earlier major deforma-

tion episode which produced major isoclinal folds. Schistosity sub-parallel ta layering in the

limbs of the major structures may belong to this earlier episode,

Introduction

Early work on the major structure of the

Broken Hill District is summarised in Andrews

(1922) and King & Thomson (1953). The min-

ing, companies in the district have also carried

out much regional mapping, some of which is

incorporated in the new map (1971) of the

New South Wales Geological Survey.

The published regional syntheses referred to

above are based on mapping. carried out before

the development of modern methods of struc-

tural analysis. They also tended to rely on the

dubious assumption that certain distinctive

lithologies (especially amphibolites and gameti-

fergus gneisses) could be treated as strati-

graphic marker bands. [t is unlikely, in fact,

that rocks of probable igneous parentage such

as amphibolites. were always stratigraphically

conformable, or that genuine meta-sedimentary

or meta-valcanic units were originally persis-

tent layers. The possibility of transposition of

Jaycring, during the complex deformation his-

tory must also be recognised, Extrapolation of

rock units through the large areas of poor ex-

posure is therefore hazardous.

Nevertheless, certain broad regional differ-

ences in rock type and in metamorphic grade

are well known, and the significance of these

has been discussed recently by Vernon (1969)

and by Hobbs e al, (1968), The review by

the latter authors offers no discussion of the

tegional structure although they make some

general comments in their discussion of the

structural history of the orehody.

Habbs (1966) and Hobbs er al. (1968) dis-

tinguish between Group One folds which have

“the widespread schistosity of the area as the

axial plane schistosity and a lineation defined

by needles of sillimanite parallel to the fold

axes” and Group Two folds which “deform the

oldet axial plane schistosity and often fold the

sillimanite Tineation”. Hobbs ef al. also state

* Department af Geology and Mineralogy, University of Adelaide, Adelaide. 8. Aust. 5001.

78 R. W. R. RUTLAND

that “Throughout the entire Broken Hill region

these (Group One) fold axes and the uxsso-

ciated lineation are observed to plunge fairly

consistently towards. the SW at low angles”.

On the basis of these statements. it should be

possible by making a study of schisiosity-

Jayering relationships to establish the broad

Group One structure of the region relatively

quickly, and the present study was. made to test

this possibility. [t was recognised, however. that

there might be more than one period of schis-

tosity formation in the region and that Group

One folds im one locality might be of the sume

age us Group Two folds im another. It was

decided therefore to try to provide continuity

of data on the style and complexity of deforma-

tion for a transect right across the region. I[t

wus thought that this would permit structural

and metamorphic correlations ta be attempted

and would serve to indicate productive lines

of further research. The method used would

not be very useful if transposition were of great

importance so that bedding and schistosilty

were often parallel and facing variable.

The transect chosen for study (Figs, 1 and

2) lies between Mt, Franks and The Sisters.

aid thus runs from lower grade, amphibolite

facies, rocks in the West to granulite facies

rocks in the east (Binns 1964), In this tran-

sect there is relative continuity of outcrop, The

transect was divided into sub-areas which were

studied by Honours students working in pairs

under the writer's supervision, Study was con-

centruted on the metasediments and in parti-

cular on schistosity-layering relationships.

te FUROR META Ws

[3t3¢

—

——Y-—. Syaciine

| —S— Antictine

aya!

South Wales

South Aust al =

Hew

Locality map to shaw the area of the

transect studied (Fig. 2). The approxi-

mate axial traces of folds postulated by

King & Thomson (1953) are shown.

R = Mt, Robe Syncline; A = Apollyon

Anticline; S = Stirling Vale Synclme:

OW and CE — Corruga West and Cor-

ruga East Anticlines.

to SANCO LLEN

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Srructura/ Clements of @ Fruntecr of @roken Hill Asgron wetween Mount Fronaks and The Sisters

Fig. 2

the data collected in each sub-area (Fig. 3).

Structural elements of the transect. The elements shown are representative attitudes based on

MAJOR STRUCTURES IN THE WILLYAMA COMPLEX 9

Schistosity-layering intersections were men-

sired or calculated at numerous localities und

can be compared with independent measure-

ments of Group One wand Group Two fold

uxes and lineations, The work was of a recon-

Naissanee nature only but Ie has produced in-

teresting new results which have provided the

hackeround for the further work now in pro-

uress.

Structural elements

It ss believed that most of the /ayering mea-

sured in the meéta-sediments corresponds to

orginal bedding (S$). This is clear when the

lithological variation is considerable and when

the layering lies at a significant angle to the

schistosily. Often, however, the layering and

schistosity are vinlually parallel and some

transposition may have occurred,

Metamorphically produced layering is usu-

wy characterised by a regular alternation of

two, and only two, distinct litholagies. Com-

monly, for example, thin mica- or umphibole-

tich laminae are separated by thicker quarto-

feldspathic laminge. Such a metamorphic layer-

ing was sutaly observed in the meta-scdiments

and then was parallel to the main schistosity,

The main urea of Granite Gneiss cust and west

of Britannia and Scotia is also characterised by

such a layering and Jocally this layering has

become involyed in Group One as well as

Group Two folds. It is not strictly parallel to

the main schistosity and thus appears to pro-

vide evidence for a metamorphic deformation

episode eurlier than the main schistosity of the

area. It is proposed to make uw separate special

study of the granitic gneisses in the transect

studied.

Schisrasity has a remarkably similar atlitude

over the whole region, Schistosity layering in-

tersections often do not correspond with Group

One fold axes or lineations however, and It

seems probable that the deformation respon-

sible for the present schistosity attitude was

superimposed on earlier deformations, Locally

therefore the main schistosity (S,) may rep-

resent 4 but little modified carticr schistosity.

Folds of a later episode which are generally of

Group Two style alsa locally develop a new

saidl plane schistosity (S.} of similar attitude,

Thus the schistosity of the region although of

fairly constant attitude may be the composite

result of at least three deformation episodes,

(There is ulso fourth schistosity developed m

the retrograde schist zones.)

Folds can be classifird into three geometrical

types uccording to their relation ta the local

schistosity. Group 1 and Group 2 folds are as

defined by Hobbs (1966) excepi thal it is not

implied, as required by the definitian of Hobbs

ed al, (1969) that mineral Jincations are paral-

lel to Group One fold axes and indeed this is

often not the case (Rutland 1969. Anderson

1971). Folds earlier than Group One can

scurcely he recognised if the Group One schis-

josity is parallel to their axial planes but where

the schistosity has been superposed ucross their

wrxial planes, they can be distinguished as

Group Nought felds-

In any one locality the age relations of the

three groups of fulds are clear but cdetermina-

lion of aye telathonships over a larger area

depends on the correct identificution of the

associated schistasity, TE most Group One folds

are related to a single deformation episode

{D,) responsible for the main schistosity (Sy }

there may nevertheless be earher Group Onc

folds (D,) where an caclier schistosity (S,))

has been preserved and later Group One folds

{D.) where a new schistosity (S,) has locally

obliterated the main schistosily,

Major structures

The sinicture of the transect studied is do-

minated by a major Group One syntorm, here

called the Parnell Synform (Fig. 2) since it

appeat's to correspond with a fold recognised

on different grounds, and named the Parnell

Syncline by Cordwell (unpublished map for

New Cansolidated Goldfields, 1962). The axial

Irace Hes betweeli the Corruga West and Cor-

ruga East anticlines of King & Thomson

(1953), In ihe east the hinge of a Group One

antiform complementary to the Parnell Syn-

form has been recognised and is here called

the Mt. Vulcan Antiform. According to Cord-

well it represents the northern end of his Dar-

ling Range anticline (the Darling Runge Basin

of Andrews (1922)),

in the west the transect has been extended

only as far ay Mi. Franks. North and west of

Mt. Franks, Anderson (1971) hus mapped a

major structure. the Mt, Robe synform which

falds the only schistasity recognised im the

area. However, no clear evidence has been

found for a major antifarm between the west

limb of the Parnell Synform and the east limb

of the Mt. Robe synform although King &

Thomson (1953) show an anticline in this

region (Fig, 1}. the Apollyon anticline, which

they describe (p. 550): only as a “broad {l-

St) R. W. R. RUTLAND

defined anticlinal structure”. Elucidation of the

relationship between the Parmell and Mt. Rohe

synforms, which may be a faulted relationship,

must await the further work which is now

Planned, In the most westerly sub-area mapped

the lavering generally dips east across a steeper

schistosity and thus it appears 10 correspond

to the west limb of the Parnell synform.

In Fig. 4 the angles of dip of Jayering and

schistosily of individual localities are related

to cach other. It emerges that in the region be-

iween the axial traces of the Mt. Vulcan and

Parnell folds, both schistosity and layering tend

to dip west, but the schistosity fs steeper than

the layering (Fig. 4b). Across the hinge zone

of the Parnell synform both schistosity and

layering change altitude so that in the west

limb the schistosity dips custerly more steeply

than the Inyering (Fig. 4c), Similar changes

take place across the hinge zone of the ML.

Vulean antiform (Fig. 4a), The schistosity is

therefore not strictly axial plane but is a gen-

erally congruous divergent type in both unti-

forms and synforms, It is therefore clear that

this schistosity (defined as $,) was generated

during the formation of the Parnell Synform

and Mr. Vulean Antiform,

It showld be noted, however, that the obser-

vations plotled in Fig. 4 are biased in favour

of Ipcalities where a clear difference in attitude

berween layering and schistosity was observer,

In many localities, especially in the east limb

of the Parnell Synform and in sub-area I of

jhe west limb, layering and schistosity are

nearly parallel, The Parnell Syntorm, how-

ever, is a relatively open structure so that these

relations are perhaps not fully explained by

the divergence of the S, schistosity. This work

Lberefore suyvests the possibility. that the schis-

tosity parallel or nearly parallel to Jayering

may represent a but little modified earlier schis-

fosily (3,) corresponding to an earlier defor-

matian episode)

Analyses of the structure of the Broken Hill

Tegion hive suggested the presence of vurious

other major folds in the limhs of the Parnell

Synform. Some congruous subsidiary folding

has beea recognised on the limbs of the Syn-

form but in general, if major folds such as the

postulated Corruga Hast and West anticlines

exist in this transect (Fig. 1), the schistosity

layering relationships suggest that they must he

of an earlier generation (i.¢, D,) than the

Group One Parnell Synform (D,) and its as-

soctaicd S} schistosity,

For the purpose of further description the

transect has been divided into four wnits, viz:

(1) The Sisters-M1, Vulcan area: the Mt. Vul-

can Antiform

(2) The Maybell area: The Parnell Synform

(3) The Springs-Old Mc. Gipps area

(4) The Mt. Pranks area.

(i) The Sisrers-Ms. Vulcan area; the M1.

Fulcan Antiform

This area is occupied hy a group of fairly

uniforms quurtco-feldspathic xemi-schists, poor

in mica. Neither layering nor schistosity is well

developed so thin collection of structural data

is difficule, Amphibolite bands occur focally

and appear to be roughly confarmable and the

group has been intruded prier to the develop-

ment of the main schistosity by a roughly con-

cordant body of coarse granitic gneiss with

lurge feldspars.

The main antiformal hinge zone has been

recognised in the area WNW of the Sisters in

a km wide belt close to the Terrowangee un-

conformity (Sub-area IV, Fig. 2, and Fig. 5),

The antiform bere is clearly a Group One

structure with nearly vertical schistosity of

similar strike on both sides of the uxial trace,

The diagram (Fig. 3, sub-area TX) of poles

f the layering indicates 4 northerly plunge of

about 40" in general agreement with ihe trend

of miner Group One folds, The main schis-

tosity of this Group One antiform will be de-

fined as S, and the oge of the schistosity in

other localities will be discussed with reference

to it.

The Sisters Synform which is clearly out-

lined by the Quartz-magnetite rock mentber

fsee Figs, 2 and 12, King & Thomson 1953)

may be a complementary synform to the Mt.

Vulean Antiform or, more probably, an carlier

isoclinul fold on which the §, schistosity has

been superposed, The schistosity in the western

limb of The Sisters fold appears to be appro-

priate for a congruous axial plane schistosity

but the near verlicul schistosity does rot

change in altitude across the hinge of the fold,

and thus crosses both limbs (which both dip

cast} im Lhe same sense, A complicating factor

is that the schistosity must have undergone

some modification during the defermation

which produced the parallel cleavage in the

overlymy Torrowangee. but it does scem likely

1 A cleur case for two episodes of high-grade schistosity formation based on superposition has now

heen established from subsequent work in adjacent areas (Rutland er ai. in preparation).

DIP OF SCHISTOSITY DIP OF SCHISTOSITY

DIP OF SCHISTOSITY

MAJOR STRUCTURES IN THE WILLYAMA COMPLEX 81

SUB-AREA Vii} 50 we *

as °°

Le EAST LIMB

* aie oa MT. VULCAN

+ So e

- 70% ANTIFORM

a Q 2" ‘a °

" reo. ‘

70 50 30 10

WEST LIMB ,

MT. VULCAN ; uA ms a

ANTIFORM #3 50

SUB-AREAS V & VII a4 /

“

=| EAST LIMB ye FS

$| PARNELL *. ‘

SYNFORM /. b

. A 50

SUB-AREA IV \ 506 i ; WEST LIMB

ie / PARNELL

SYNFORM

Easterly

EAST LIMB

10 .

PARNELL

SYNFORM P 7 a

Westerly

Westerly Easterly

DIP OF LAYERING

Fig. 4. Relative dips of layering and schistosity.

= RK. W. KR. RUTLAND

that the Sisters fold is of an earlier generation

than the Group One Mr. Vulcan antifurm and

the associated S, schistosity, and there is clear

evidence of minor folding earlier than the

schistosity..

Most minor folds in the hinge of The Sisters

synform are Group One structures of distinctly

Variable mortherly plunge, One excellent ex-

ample of earlier minor folding occurs on ihe

hinge of u Group One structure, The earlier

fold on which the schistosity has been super-

posed has a nearly horizental plunge and an

east-north-east trend. Conceivably therefore

the main Sisters fold is a reclined carlicr struc

ture on which the mami schistustty and usso-

ciated Group One minor folds have been

superposed. Vernon (196%, p. 52) also notes

that “small isolated jsoclinal fold hinges in

quartzite fxyers can he traced around the

hinges of the relatively large folds” at the Sis-

ters.

Further south in the traverse ESE of the

Springs H.S. (sub-area VIIL, Fig, 2) a Further

complication occurs with the recognition of

two schistosities. The muin schistosity generally

dips north-west in the western limb of the Mc.

Vulcan antiform. In the north draining valley

about two miles east of the Springs H.S., how-

evec, both the layering and this schistosity are

folded round the hinge of an antiform whieh is

therefore Group Two with reference to this

schistosity, A new schistosity is locally deve-

foped in the Hinge, however, so that with

reference to the later schistesity the fold is

Group One.

Ik is not clear which of the sehstosines

should he correlated with the single prominent

schistositv immediately to the north. If the

earlier schistosity is so correlated (as is fay-

Oured by its intensity) then it may be described

as 8, and the Jater schistosity can be regarded

asa loeul development of S.. Lf, however, the

Jater schistosity is correlated with that to the

north (as is favoured by their orientatians)

then the earlier schistosity must be regarded

as one preserved from an euslier period of de-

formation, ic, it would be an S,, schistosity.

Purther work is needed to determine unequi-

yocally whether the major antiformal structure

in refiuled to the earlier or the Inter schistosiry

but the seoond alternative is here preferred,

Further south again in the traverse between

Razer Back and Moorkaie the schistosity-

luyertny relations indicate the presence of o

Grup One synformal structure east of the

fai uniform (Fig. 2), West of the Springs

H.S., however, layering again dips west more

gently than schistosily and the Moorkaje syn-

form is therefore regarded ag a relatively xub-

sidiary fold on the west limb of the major Mt.

Vulcan antiform.

It is notable that both Group One and

Group Two folds and lineations in this region

have northerly plunges (Fig, 3, swb-areas WIT.

VITT and EX). Schistosityayering intersections,

however. are much more vuriable and may

have any plunge within the NE striking zone

corresponding to the general allitude of the

schistosity.

Tt is inferred, therefore, that the Mt. Vulcan

antiform as defined, is a Group One structure

superposed On tsoclinal folding represented by

the Sisters Synform. It is evident from the

relations desenbed, however, that this Group

One structure could correspond im aye to

Group Two structures elsewhere, which fold

an carlier schistosity. It cannot be assumed that

the antiform is an anticline or that it folds a

simple succession of constant Facing,

(2) The Maybell areat the Parnell Synform

The hinge zone of this structure occurs in

sub-area IV in a group of mica schists with

quartzite and quarty-rich gneiss interbeds, Both

schists und gneisses are commonly garnet-

ferwus.

The well-developed lavering and schistosity

in these rocks has facililated folding which is

tighter and of smaller wavelength than in the

Mt. Vulcan antiform. The hinge zone is made

up of several folds so that the main axial trace

is not easily drawn without detailed mapping

(Fig. 6). The map suggests that the axial trace

has suffered some right-lateral offser on the

ENE trending shear zones which cross the area,

The diagram of mesoscopic data for this

structute (Fig, 3, sub-urea TV) is somewhat

diffuse so that a plunge variation from gentle

north to gente south can be inferred, At least

part of the spread is due to Group Two folds

aml these generally plunge to the south. The

main fold, however. is clearly a Group One

structure and minor Group One folds more

commonly plunge to the north (Fig. 3). Bvi-

dence along the main hinge line in the northern

part of the area for example gives a plunge of

16/020 while dextrul folds on the west side

of the gneiss in the south of the area plunge

$4°/028. A few hundred yards west of the

latter outcrop, however. Group One folds in

interbedded qnartzites and schists plunge 30"/

196, Mineral lineations have occasionally beca

observed to plunge north at moderate pngles

MAJOR STRUCTURES IN THE WILLYAMA COMPLEX

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ADUEH OG PUP UOTE y ‘seuZNOD'g ‘Vojdweg'y aly

MSN TWHH NavYOud

V3HV SYSISIS,-—SONIddS SHI, 40 Lewd

SONIMOHS

hy. dV¥W IWHALONYLS

se 9 Fone”

sive pyo, yz dnoig .

BulaaAeq

Ayiscysiyog =

Saul) Buat, So -

Ppas!)P2aua9 No

4 Ro WOR. RLTLAND

in both limbs of the major structure but others

have been obseryed to plunge gently to

moderately south.

The Jayering-schistosity intersections again

show much greater variation than the fold axes

(Fig. 3). This shows that strain axes and peo-

Metric symmelry axes were not coincident and

suggests that the schistosity may be superpased

on i complex and possibly pelvphase fold sys-

lem, The clearest evidence of this ts in the pre-

sence, in the gneisses, of what appears to be u

melamorphically produced Javering which has

been folded with the main schistosity as uxial

Plane. Tf the main schistosity 1s again defined

us Sy) und the associated Group One folds as

D, then the metamorphic layering provides

evidence of an earlier Dj, metamorphic ude-

formation episode:

In sub-earca IW (Fig, 2 and Fig. 3) schistosity

and layering trends are roughly parallel,

though dextrs) relations are more commen in

the west limb amd sinistral relations in the east

limb, suugesting « closure to the nurth*. Over

a wider area, however, 4 notable feature is that

the liyering tends to show w dextral relation

to the schistosity in. both limbs of the fold, ic.

in sub-areas ILL und Vo (Fig. 2). ‘This would

imply a generally southerly plunge of the schis-

tosity layering intersections in the west limb

and a noltherly plunge in the east limb. In

fact Croup One fold axes do commonly have

a vorherty plunge in the east limb althoug’y in

sub-alreas Yoaod VI the plunges are often very

steep, Group Ong folds in the west linib (suh-

wea VW) da have a. south-easterly plunge It

can be inferred therefore that the schistosity

lies slightly incongruously across the structure.

though Lhe divergent attitude ef ihe schis-

tosity with respect to the axial plane confirms

That the major structure and the schistosily are

Beneticully rehited,

The limb areas of the Parnell Synform ure

Jiscusseed tn more deta! below

(A) Pie Sprentge-Oled Mt. Gipps arent

Schistosity and layering are offen nearly

purailel in this area bute where their dips have

heen distinguished the layering generally dips

west less steeply than the schistosity, The schis-

losity-luyering intersections show the usual

vanation in i NE trending great cirele, In sub-

urea V (Fig, 3) the schistosity-layvering inter-

sections more commonly plunve steeply ta the

south us do observed mineral lineations in the

schists. Group One fold axes, however, vury

from steep south-eusterly plunges to ‘steep and

moderate northerly plunges while Group Two

folus vary from steep southerly to stecp mor-

therly plunges. On the eust side of the main

franite-gneiss body, however, in the schists of

sub-aren VIL (Fig. 3) schistosity-layering inter-

sections plunge less steeply cither NNE. or SSW

and observed Group One fold axes have exclu-

sively NNE plunges. This contrast between the

variable plunge of schistogity layering inter-

seclions and the mofe consistent plunges of

Group One fold (xcs is similar to thal already

neled for the hinge area of the Purnell swoforin

abd reinforces the suggestion that the main

schistosity is slightly oblique om the major

simucture.

In the cast limb of the Parnell Synform no

euther major folds (Group Nought) have heen

recognised hut if the folds postulated by King

& Thomson (1953) and Cordwell (unpublished

mup for New Consolidated) Goldfields. 1962)

cxist they would belong in this category, Brief

coniments. On these postulated folds ure mace

helow,

(a) Tue Muiaas Syncrine,

This fold was inferred to lie with uw NNE

trending axial trace in the schists in sub-are:

VIL (Fig. 2) east of the miin body of eranite

gneiss. There is no evidence of repetition of

the sticcession in the meta-sediments on either

side of this trace although the acromugnetic

map <loes sugpest the possible repetition by

folding of the distinctive quartz-magnetite rock

unit. Boudics of granite gneiss da flank the

schisis un both sides of the proposed fold bul

this rock type is probably intrusive, although

it was emplaced before the development of the

muin schistosity, Layering ind seistusity are

oflen nearly parallel in this area and schis-

tosity-layering intersections may plunge either

north or south, Where distinguished, however,

the layering dips west more vently than the

schistosity. Thus the area of this postulated fold

lies wholly in the western limb of the main Mt

“Phe sehiitosity-layering relationship is described as dextyal when the layering trace in pralite tor

on a horvzontal surface! fs clockwise fran» the schistosity wace. This any minor tuck or “drne”

folita toowhich the schistosity is wsial plane are also deaxtral and have a dexeral schistosity-livering

relalionshife ins their long limbs. Conversely the schistosity-layering relationship is described as

sinisual when the Jayerme trace In prohle for on 4 horizontal surface) is anticlockwise frou the

schistosity trae.

MAIGR STRUCPURES IN ‘THE WILEYAMA COMPLEX RS

Vulcan antiform ane, if it exists, it is earlier

that the axial-plane schistosity of hat Fold.

(tb) Yanco ANTICIINE

The main outerop of granite gneisses north

of Britannia and Scolia was inferred co lie in

the core of an anticline. Southwiirds this Yanco

anticline was supposed to be divided into two

subsidiary anticlines (occupied hy the two

southerly projections Of granite gneiss), sepa-

rated by a syneline of metusediments south of

Britannia and Scotia mine. Insufficient data has

been wathered to evaluate this hypothesis fully

but several relevant poinis can be made

(Fig. 7).

The granite gneisses display a complex inter-

layering with the metusediments, w relationship

which may be primary or due to subsequent

deformution, There is evidence of three defor-

mation episodes in the gneisses. The main

schistosily S,; (D, deformation) is superposed

on ao earlier metamorphi¢ layering in the

eneiss (D,,) and it is tolded into Group Two

folds (Do). The prominent southerly Jineauion

may be related to D, or D,.

A Group Two fold of more than one hun-

dred metres wavelength occurs in granite

gneiss ahour 1500 m south of old Mt. Gipps.

This is a large sinistral parasitic fold with a

soulherly plunge on a general westerly dip.

Other Group Two folds are dextral with oor-

therly plunges but all are parasitic folds and

there Is no evidence of any major Group Two

fold which might repeat the succession.

Schistosity-layering relationships are com-

plex: venerally schistosity and layering are

nearly parallel aod the attitude of their inter-

sections is very yuriuble: where the ungle he-

tween schistosity and layeting tx substantial the

achistosity generally has the steeper westerly

dip but in some cases the layering dips casi-

watds less steeply than the schistosity, This

suggesis The presence af sume Group One falds

and a chear example. dextral with northerly

plimge, cin be seen nearly 3 km NE of

Old Mt. Gipps. Again, however, no systemutic

vanation in schistasity-layenng relations was

found which might indicate a majur Group

One fold and in general the layering dips west

more gently than schistosity on both sides of

the main granite-gnems outcrop, It is therefore

inferred that. if the eranite-gnciss areas do tie

mm the hinges af major folds, such folds must

be earlier than the Parnell Synform and Mt,

Vulcan antiform, No positive evidence for such

folds bas been found bur Curther study of vhis

aréa is required

(7) NINE-Mi.e SYNCLINE AND MAYREDI

ANTICLINE

These fulds were inferred by Gordwetl in

the essentially metasedimentary aren west wf

Old Mi. Gipps (the Maybell anticline carres-

ponds approximately to the Corrusu Rast unti-

cline of King & Thomson 1953). They were

apparently based partly on the suppased repe-

tition of amphibolites and of a para-gneiss unit.

These repetitions have not heen substantiated

hy the present work. Distinctive lithologies af

pale calcareous schists occur along the old

tramway north-wesl of Old Mt. Gipps and

these have not been found further west.

However, schistosity and layering shaw a

variety of relationships although in general the

layering dips west more gently than schistosity

ina dextral relationship and phinges are nor-

therly (Fig, 7). Along the old tramway, haw-

ever, the layering dips east more gently than

the steep schistosity and the prominent Grougr

One folds ate dexttul on a southerly plunge (ys

in the west limb of the main Parnell syntorm),

There is some inconclusive evidence in these

outerops that the Group One folds refold un

earlier set of Group Nought folds. These rely-

tions of Group One structures surgpest the pre-

sence of uw minor dependent antifarm in the

cast limb of the main Parnell Synform, but, us

with the major structure, the plunge yarition

suggests that the schistesity is oblique to the

axial plane of the fold.

(4) THe Mi, Franxs Ages

Tn sub-areas Wf and 1 the layering generally

dips east more vently than the schistosity in a

dextral relationship an a southerly plunge,

often steep. This is especially well seen in a

coarse schist unit defining a number of cextral

folds in the ares south of Florida Mine. There

is sone evidence that this anil closes sourh-

wards in a major fold wih a core wt Parnell

gneiss (resembling Potosi gneiss) but beth

limbs dip cast across the yertieul schistosity und

the Group One folds have the same dextral

sense in both limbs. This suygests that the pos-

sible major fokl is a Group Nought fold, with

reference to the axial plane schistasity of the

Parnell svnfarm, No evidence for the sorth-

ward continuation of the Sdrling Vale svncline

(King & Thomson 1953) was found in this

sibearca.

Tn sub-area Il the schistosity und Joyering

are generally nearly parallel and Group One

Minor folds are rare, Most commonly the

Inyering dips cast acrots f steeper schistosity in

86 R. W. R. RUTLAND

Schistosity - Layering

hinge zone of the

60 After

Fig. 6.

a de¢xtral relationship on a southerly plunge

but near the eastern margin of the sub-area

_some sinistral minor folds occur, also on a

southerly plunge since the layering here dips

east more steeply than the. schistosily. This sug-

gests the presence of an overturned south

plunging antiform-synform pair on the western

limb of the main Parnell synform. The axial

trace of the Apollyon anticline as mapped by

relationship

Parnell

in the

Synform

L.Chenoweth and L,Schmidt

A283 751

63 2

i A co

a he 8 ay. ht

V5 BS

vss ag

—- Layering

Lj} Sehistosity

4 8B wn »=ORetrograde faylt zones

a a Approximate trace of

Parnell Synform

Vabtty o ri

L 11 1 i |

ho OM bites

Structural elements in the Maybell area: the Parnell Synform.

King & Thomson (1953) runs through this

area and further work is required.

Also in this sub-area, close to the track cast

of Mt. Franks the quartzo-feldspathic sedi-

ments show a strong “elongation” Jineation

plunging south-east in relatively low angle

schistosity. These rocks are also inyaded by

abundant pegmatite and they provide a strong

structural contrast with the tocks further west,

MAJOR STRUCTURES IN ‘THE WILLYAMA COMPLEX

Possibly the lineation and the schistosity which

is sensibly parallel to layering are preseryed

from a deformation episode earlicr than the

Parnell synform.

In sub-area I there is relatively little peg-

matite and the rocks are commonly phylilitic,

though some members are rich in andalusite

porphyroblasts, around which the schistosity is

deflected, The layering again generally dips

east more genlly than schistosity but in con-

trast to sub-areas IL and IIL the relationship

is now generally sinistrul and the plunge of

the Group One minor folds is to the north,

The Jayering actually trends ubout N-S and the

schistosity about 030°.

Thus the relationships are still consistent

with a position in the western limb of the main

Parnell synform but the trend of the layering

hus changed and the plunge has changed from

southerly to northerly. These changes might be

attributed to the presence of a southward clos-

ing Group Nought fold between sub-areas I

and Jl. No evidence of such a fold has been

found and the strong contrast of structural

style between the two sub-areas rather suggests

the presence of a thrust fault.

Nearer to Mt. Franks there is a reversion

to a dextral relation between schistosity and

layermg and to a southerly plunge since the

layering continues to dip east across a nearly

vertical schistosity,

On ML. Franks itself there is a Jarge dextral

fold and crenulation cleavuge is strongly deve-

loped. It is apparent, howeyer, that the S;

schistosity which has suffered crenulation was

itself formed at a high angle to the layering.

4 _ -

IEE aT (Rad 8 EG

/, bS

/ } i Ff of ( 56 el of of! x t E | y ‘ f f

AVR Nae HONKY

NE LF INE PI ON TS 7

boa "IC Xe / wa ral la Wt (2 Me 4 \ WY , F| irs Z

io ‘ qe 4 oy Near +9 \ \ iF f af 5 / F {

a “ is ; 7 !

# \Wese AG Ps Te ) a Tee ps 2} Seat Ph - f

ae ft Op / “& Se ot wf i \ { fs

a i / LS a ein ut cies Hel f of oe

a leg AN. a ( 4) ) / f / i ah

oe , y 5 j - Bh

as} / 2

Pat AWS ¥ A i (3

f Ved a re - des

i A lp

aol FY She

os, wy \ c a toe é > ae ‘iad

by c ~ ¢ Le ¥y,

_ a ri we/ t \ fa. aa yf

~~ ey, YA to f

§ Ma ge ol af \ as {

/ = Sei)? \Y 7

ee) ‘

Pres ¥

ye |

fe so 1 }

Metres Milometees

pre Broken Hill |

=— Road >— «Group I told axis “+ Intersertion of layernny and schistosity

oe Layering > #$Groun DT told ents Rh Creriglathen cleavage

LI Sriratosiry —+ ~=Mineral broeatien ta} Areas af sa jd poet water

Fig. 7. Structural eleinents in the Old Mt. Gipps area.

8s R.

Ft is inferred therefore that the main Mt,

Franks: structure is essentially a large Group

One dextral fold modified by Group Two folds

and crenulation cleavage, As noted above, the

elucidation of the relationship. of these obser:

vations io the interpretation by Anderson

(1971) of the Mt. Robe area must awail

further work.

Conclusions

minor folds of Group Nought, Group One

and Group Two styles have been recognised

and would suggest the presence of three

periods of deformation if it is assumed that the

schistosity is everywhere of the same age. Some

doubt is cast on this assumption by the fact

that in some areas (particularly the hinge zones

of the major structures) the schistosity is con-

sistently steeper than layering and mukes a chs-

tinct angle with it while in others (especially

in the limbs of the major structures) it 1s

nearly parallel to the layering.

The Parnell Synform and Mt. Vulcan anti-

form are apparently of Group One character

since ihe undoubted $, schistosity is roughly

congrucnt and forms divergent or reversed

fans. Since the schistusity attitude varies sys-

tematically according to its position in these

folds tt seems probable that the folds and the

divergent schistosity, non-parallel to layering,

were formed during the same deformation epi-

sode, Nevertheless the fact that the layering

generally shows « dextral relation to. schistosity

in both limbs of the Parnell Synform suggests

that the schistosity has been superposed

stighly obliquely on the fold, after the initia-

tion of buckling. This oblique superposition

may be partly responsible for the difference in

plunges in the two limbs of the Parnell Syn-

form hut there is some evidence that earlier

folding is also significant.

The dominant dextral relation of layering

to schistosity sugycsts that Group One folds

related to the schistosity should plunge south-

cust in the West limb and north in the -east

limb of the Parnell Synform, In fact

schistosity-layering mtersections and fold axes

(Figs, 3 and 8) show a wide variation in att-

tude in a great circle zone striking NNE. This

suggesis that the laycring attitude on which the

schistosity was.superimposed was variable, pos-

sibly due to earlier folding. Moreover, there is

not a close correlation between the attitude of

Ww. R. RUTLAND

' ——~

4 | eh

' a

' . “a ,"

. '

“4 nf

‘ 4

/ a» ah Eee

/ Ao ? «1 7

/ os Mn \,

/ 4 ‘ =

/ . atte , ‘

{ .

ate

| . my \

| . Jt ¥ |

i a

| = ee {

. .

i} “ 4

\ “ap a4 y

' * Iai 2 Fs

i .* 3 ree

“4 5 . ‘

- «’ 4 . ‘ “ 2 \

. a . 4 - 7

oy . 2

- 4, , ¢

+ % ‘

4 *s

le 7 a Pe The

« Cevp tT tntan

Timeations

Fig. $ Lower hemisphere equal-area projection

of fold axes and lineations for the whole

Irunsect.

Group One folds and schistosity-laycriny inter-

sections, There ts a closer correlation between

layering-schistosity intersections and Group

Two folds suggesting that the latter have been

controlled by the former.

Minor folds of Group Nought character

which can unequivocally he said to be earlier

than the schistosity are rare however. The di-

vergen| schistosity inevitably approximates to

the axial plune of any eurlicr pearly isoclinal

foluls and the distinction can be made only in

areas of favourable lithology and exposure’,

I. has giready been noted, however, that un

carlicr schistosity may be preserved, and the

evidence in gneisses of u metumarphic layering

tarlicr than the S, schistosity provides con-

vincing evidence of an eurlice deformation epi-

sode. On the map-scale moreover, the Sisters

Yok and some others appear to be isoclinal

major structures earlier than the Parnell syn-

form and its related schistosity. Since the axial

planes of these isoclinal folds are approxi-

mately parallel to the limbs of the Parnell syn-

form it follows that they were recumbent

before the deformation which produced the

Parnell synform (Fig, 9),

%A good example outside the area under discussion can he seen south-east of the main road, about

onc km north-east of the Flying Doctor base, There the schistosily-layering Telationsbip is sinisuwal

and congruent Group One minor folds oceur with south-westerly plunges o! about 50". The schis-

tosity culs across occasional earlier dextral folds which plunge north-north-east.

MAJOR STRUCTURES IN THE WILLYAMA COMPLEX ay

cf PARNELL

SYNFORM

‘hrust oof

deformation

Possitie

PAbliat

Sehistosity (Sy )

cf MT. VULCAN

ANTIFORM

Axial trace of probable

wcarlier Tatds and attitude

Of #ariter sohistosity

Layering | S7

Fig 9.

Diagram to show general form of the Parnell Synform and Mt. Vulcan Antiform and their

possible relationship ta major structures of the inferred earlier generation. No attempt is

made to show specific early structures which have been postulated.

Three major deformation episodes are there-

fore inferred:

1, Dy; Formation of tight Group Nought

folds (apparently Group One if the later

S, schistosity 1s roughly parallel to the axial

pline or if 5, is preserved) including the

Sisters synform, Original attitude possibly

recumbent but now upright with steep

plunges,

D,: Development of the main folds, the

Parnell synform and Mt, Vulcan anitiform

together with their associated (S,) schis-

tosity.

3, Dy: Formation of relatively minor Group

Two folds, plunging south except in hinge

urea of Mt. Vulcan antiform.

Further work is now in progress on a fur-

ther east-west transect, immediately north of

Broken Hill. ft is hoped to test the conclusions

presented here, to extend knowledge of the

Major structures ind to correlate the deforma-

tion phases recognised with those established

by other workers (Hobbs 1966; Williams

1967; Anderson 1971).

Acknowledgements

The mapping, on which this paper is based.

was carried out by a group of Honours s{u-

dents of the School of Geology, University of

Adelaide in May, 1969, under the writer's

supervision. The students were Messrs. K. F.

Bampton, T. H. Bell, L. M. Chenoweth, D. A,

Couzner, T. M. Clifton, N. J. Crase, R, A,

rears, D. N. Harley, P. G. Haslett, A, N,

Larking, H. Mastins, R. K_ Netzel, P. R.

Pierce, L. E. Poole, B, V, L. Rees, P. W,

Rooney, B. L. Schmidt, R. E. Williams, A

preliminary version of this paper was circulated

as Rescarch Report No. 1 of the Centre for

Precambrian Research, University of Adelatde,

1969.

Financial assistance from the Broken Hill

Mining Managers Association is also gratefully

acknowledged.

References

Anpbrerson, D, FE. (1971).—Kink bands and major

folds. Broken Hill, Australia. Bull, geal, Soc.

Am. 82, 1841-1862.

Anprews. E. C. (1922).—The geology of the

Broken Hill district. fem. veo! Surv. NSW

Binns, R. A. (1964).—7Zones of progressive re-

gional metamorphism in the Willyama Com-

plex, Broken Hill district, New South Wales.

J, geal, Sac. Aust, U1 (2), 283-330.

Gusrarson, J. K., Burrete, H. C., & Garretry,

M. D. (1950), —Geology of the Broken Hill

deposit, Broken Hill, N.S.W. Bull. ecol. Soc.

Am. 61, 1369-1438.

Hoss, B. FE. (1966)—The structural environment

of the northern part of the Broken Hil! ore-

body. J. geol. Soc. Aust. 13 (2), 315-318.

Hoses, B. E., Ransom, D. M., VERNON, R- Hi, &

Winteiams, P. PF. (1968).—The Broken Hill

Ore Body, Australia: a review of recent

work, Miner. Depostta 3, 293-316.

90 R. W. R. RUTLAND

Kine, H. F., & THomson, B. P. (1953).—The

geology of the Broken Hill district. Jn Geo-

logy of Australian Ore Deposits. Prec. Fifth

Emp. Min. Metall. Congr., Australia and New

Zealand, 1953 1, 533-577.

Ramsay, J. G. (1967).—“Folding and Fracturing

of Rocks.” (McGraw-Hill.)

RuTLAND, R. W. R. (1969),—Relations of struc-

tural elements in a transect of the Broken

Hill Region. Centre for Precambrian Re-

search, University of Adelaide Research Re-

port No. 1.

Vernon, R. H. (1969).—Archacan or Lower Pro-

terozoic rocks. The Willyama Complex,

Broken Hill area. Jn G. H. Packham, Ed.,

“The Geology of New South Wales”. J. geol.

Soc, Aust. 16(1), 20-55.

WILLIAMS, P. F. (1967).—Structural analysis of

the Little Broken Hill area, New South Wales.

J. geol. Soc. Aust. 14(2), 317-331.

THE SYSTEMATICS OF SOUTH AUSTRALIAN PRECAMBRIAN AND

CAMBRIAN STROMATOLITES. PART II

BY W. V. PREISsS*

Summary

PREISS, W. V. (1973).- The systematics of South Australian Precambrian and Cambrian

Stromatolites. Part II. Trans. R. Soc. S. Aust. 97(2), 91-125, 31 May, 1973.

Five new forms of stromatolites from South Australia (nzeria conjuncta, I. multiplex, Jurusania

burrensis, Katavia costata and Kulparia kulparensis) are described. South Australian occurrences

of Conophyton garganicum garganicum, Gymnosolen cf. ramsayi and Inzeria cf. tjomusi,

previously known from the USSR and elsewhere, are also discussed.

THE SYSTEMATICS OF SOUTH AUSTRALIAN PRECAMBRIAN AND

CAMBRIAN STROMATOLITES. PART II

by W. V. Preiss*

Summary

Premss, W. V. (1974).—The systematics of South Australian Precambrian and Cambrian

Stromatolites. Parl If, Trans. R, Sac, S. Aust. 97(2), 91-125, 31 May. 1973.

Five new forins of stromatolites from South Australia Umnzeria conjuncta, I. multiplex,

Jurusania burrensis, Kaiavia costatu and Kylparia kulparensis) are described. South Australian

cccurrences of Conophyton garganicum gurganieum, Gymnosolen cf. ramsayi and Inzeriw cf.

tjomusi, previously known from the USSR and elsewhere, ure also discussed.

Introduction

“This paper is a continuation of Preiss (1972)

in which the principles of stromatolite classifi-

cation were outlined and several new forms of

stromatolites were described, The glossary ap-

pended fo Part I also applics to this paper.

Systematics

Group CONOPHYTON Masiov

Conophyton Maslov 1937. 334, Koralyuk

1963: pl. 5, Fig. 3. Komar, Raaben & Semi-

khatov 1965; 27, Kamar 1966: 72, Cloud &

Semikhatov 1969: 1037. Bertrand 1968: 170.

Walter 1972: 102.

Type Form: Conophyton lirietn Maslov,

from the Dereynin Suite, Lower Tunguska

River,

Diagnosis: Non-branching or extremely rarely

branching columnar slromatolites with conical

laminae, usually thickened und/ear contorted in

their erestal parts,

Content: C, cylindricunt Maslov; C. pietu-

lunt Kirichenko; C. cireulum Korolyuk:

C. garganicum Korolyuk; C. mileradoyict

Raaben; C. Jitu Maslov; C. baculum

Kirichenko; C. gaithitza Krylov; C. ressoti

Menchikolf; C. cadilnicus Koralyuk and

C, confertum Semikhatov.

Conophyton varganicum garganicum Korolyuk

(emend.)

FIGS. 1. 2a. 9a, 13, 12a

Conophyron cf. garganicus (partim),

Glaessner, Preiss & Walter 1969: 1056,

Material: Eleven specimens from Paratoo,

S. Aust.

Description

Mode of Occurrence: These stromatolites have

been found only in a diapiric raft in the Para-

too Diapir. The basal portion consists of flat-

laniinated stromatolite, passing up into large

domal structures up to 1 m diam. (Fig. 11¢).

Domes are usually laterally linked, occasion-

ally separated by small interspaces, then divid-

ing into discrete columns, 1540 cm in diam,

with conical laminae, Transverse sections of

columns round to oval or lanceolate (Pig.

Jib). Columns 1-4 cm apart, with some mas-

sive bridges, often slightly bent, with axes non-

parallel, diverging at up to 30° (Fig. lla).

Some of this divergence may be due to tec-

tonic disturbances. The original mode of occur-

rence is not clear because of the discontinuous

outcrop, it may have been a bioberm or thick

biostrome, perhaps. 30 m thick. The only evi-

dence ag to the facing of the bed is the upward

passage from flat-laminated to conical stroma-

tolites, with apices growing upwards,

Column Shape: Ficld observation shows that

columns are somewhat irregular cylinders, with

ragged edges, massive bridges and overhanging

laminae. Only one specimen was suitable for

reconstruction (Fig. 2a). Columns of round

transverse section haye a linear crestal zone,

while those of elliptical and lanceolate sections

have crestal plunes in the long axis of the

ellipse (Fig. 11b), Specimens studied in the

laboratory also show both types.

* Geological Survey, South Australian Department of Mines, Box 38, Rundle Street P.O., Adelaide

5000.

92 W, V. PREISS

‘The margin structure is very irregular. with

numerous large bumps, overhanging peaks and

shore cornices. (Pigs, 2a, lta). Bridges vary jn

thickness from one Or two to several lens of

laminae,

Branching: No true branching except actual

separation of columns from the domed and

flat-laminated base, Rarely a small projection

with convex, non conical laminae occurs. on

the margin of a column,

Lamina Shape: In longitudinal axial sections

laminae steeply conical, apical angle generally

acute (50-90°) but obtuse angles cecur near

the base of the columns, Away from crestal

zone, laminae usually straight and parallel in

longitudinal section, but in places bent down-

wards near the column margins, producing a

shupe resembling gnthic arches (Fig. 94),

Crestal Zone: All laminae more or Jess thick-

ened in crestal zone. Some light laminae

greatly thickened. Dark laminae arched up and

contorted, often leaving irregular voids filled

with sparry dolomite, within the thickened

light laminae (Fig, 11f), The erestal line, join-

ing apices of successive conicul laminae, is

very wavy, with frequent sharp displacements

of crests (Fig. aj, The overall shape of crestal

zone ts however straight (Fig. 12a); ir corres-

ponds mostly to Type HI (after Komar,

Raahen & Semikhatovy 1965, p. 23, Fig. 5)

with uneven thickenings and sharp lateral dis-

placements, but some examples of Type Il

(without lateral displacements) occur. In

places, laminae are deflexed immediately out-

side the crestal zone (Fig. !2h). The diameter

of the erestal zone is ken os the width be-

tween the limits of thickening of laminae, Out

of 33 measurements, 63% Jie between 7 and

9mm, 24% between 5 and 7 mm, and 12%

betwecn 9 and 12 mm.

Lamination; Very distinctly banded and

striated in better preserved specimens, consist-

ing of straight, parallel, smooth, very thin

laminae, either very continueus, or formed by

chains of elongated lenses, aligned in definite

layers (Figs. Tle, 11f), Two types of primary

laminae occur: light { L,} and dark (L.). In

some specimens 1. layers grouped inte fairly

Uistinct macrolaminae, in Which light laminae

are thin and subordinate, separated by layers

of predominantly L,; iype (Fig. 11f), The ap-

pearance of macrolaminae has been eNxag-

weraled by the preferential recrystallizatinn of

light laminae. L, taminae relatively pure and

transparent, mostly 0.08—-0.1 mm thick, gen-

erally of very constant thickness from the else

of the crestal zone to the column margin, never

lensing out. They are internally homogenous.

composed of xenolupic. almost equigranular

dolomite, of grain size from O.1H—-0,03 mm.

Many grains slightly incquidimensional. Occa-

sional lenticular spay-filled cavities have dark

laminae draped arvund them Fig. lle), L.

laminae darker, much fess transparent and

samewhal finer grained than L, laminae, the

Fine crystals stained by 3 pale brownish. pos-

sibly organic coloration (Fig. 1le). Mast dark

laminae 0.02-0,10 mm thick, ont os continuous

as L, laminae, frequently splitting into series

of lenses, 0.2-1.0 mm Tong, and 0.1—1.0 mm

apart, aligned parallel and separated hy pale

laminae. Some dark laminae ure continuous for

several cin; some have slight, rounded, lenticu-

jar swellings, These, as well as the lenses, may

be blunt ended, rounded, or pointed, Rarcly,

they contain significant swellings, the under-

fying ynd overlying jaminae heing draped

around them. Relatively large (0.52.0 mm)

neduies, within.a pale lamina (eg Fig. Ie)

are probably detrital carbonate grains, 1... Ia-

minac composed of equidimensional. equigra-

ular, Xenntopic dolomite, of grain size 0,006—

0.015 mm. Boundartes of L, and L, laminae

distinct and smooth, but slight recrystallization

has made them a little diffuse in plages. Mac-

rolaminac, consisting of sets of Ly laminae.

very prominent in some specimens, are U.4—-

1th mm thick, composed of 5-10 Ly-L. Ia-

mination pairs, bounded by predominantly

light macrolaminae (.2-0.5 mm thick. often

spurry and recrystallized (Fig. 11f),

Statistical Study; Numerous measurements

were made on six large thin sections, of the

following parameters: (1) thickness of light

laminae I,; (2) thickness of dark laminae L..;

(3) ratio of thicknesses of adjacent dark and

light laminae La/L, and (4) coeficient of

thickening. i.e ratio of thickness of a lamina

in crestal zone, to thickness of same lamina

outside crestal zone.

The distribution of thicknesses ef Jarninae

L, and L., were plotted graphically for thick-

ness Intervals of 0.02 oun; the [requencies of

intervals were plotted against the mid-point of

each interval, for the six specimens (Fig. 1b

to g). A comparison of the six graphs for each

lamination type shows some variation between

specimons, especially for L. laminac, which is

interpreted as being due to the difficulty of

distinguishing single datk laminae and the

thinner macrolaminge in same specimens, This

difficuity is increased with rreater recrystalliza-

lion, so that one would expect the more re-

SOUTH AUSTRALIAN

STROMATOLITES IL 93

Fig.

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S.A. Department of Mines

1. Diagnostic characters of Canophytan: (a)—The traces of the crestal lines of two specimens

(S214 at left and $532 at right) drawn from thin section (x1/3); {b) to (g)—Frequency

distributions of thicknesses of light Jaminae Li and dark laminae Le» for 6 separate speci-

mens; (h)—Pooled frequency distributions of lamina thicknesses for all six specimens, com-

pared with data for Russian conophytons; (i)—Frequency distribution of the ratio of thick-

nesses of adjacent dark and light laminae (La/Li), pooled for all specimens, compared with

data for Russian conophytons; (j)—Frequency distribution of the coefficient of thickening

of laminae in the crestal zone. compared with Russian conophytons; (k)—Comparison of

contour diagrams of the frequency distributions of dark and light laminae (contoured in num-

bers of readings),

93 W. V. PREISS

crystallized specimens to have proportionately

more numerous thicker Jaminae (actually thin

macralaminae), Le. the mean thickness should

be higher than for less recrystallized ones. The

following table Compares meun thickness (in

mm) af L, and Lo with degree of recrystalli-

zation observed: L. means have much ureater

spread about the total mean then L,, and the

highest means of L. correspond to the most

recrystallized specimens.

Degree of

Specimen Reerystal-

number L, méan La imean lization

S214 0.128 0.073 Well preserved

$213 0.107 0.066 Slight

S278 0.145 0.065 Slight

S277 OAL 0.084 Sticht

§32 O15 0.089 Strong

$43) D.DST 0.134 Siraug

Total inealh = D6 0,085

The data for the six specimens were com-

hined, replotted, and compared with the dis-

iibution curve of the Russian Conaphyior

gargenicum garganicun. (Fig, Thy. While the

Lo curves are very stnilary L, has a higher

mode in the South Australian form (0,08 to

1.10 mm), with asceondury peak tn the mter-

val 0.04 to 0.06 mm, which characterized the

Russian form, To some vxtent. the bimodality

ig due te errars of mevsurement arising from

the judgement ul lamina thickness sehilive to

the scale of the graduated cyepiver, and to the

Presence of thinner macrolaminse ws discussed

above,

Rate Lyth,y for Adjacent Laminac; Results

from all six specimens were pooled and plotted

in intervals of 0.25. Fhe graph compares very

closely with that of the Russian form (Pig. 11),

The dain may also be represented in the form

nf « eoutoured frequency divgram of LL.

avainst Ly. The shape and position of the

maximum are compared with those of con-

toured Russian plots; they diller only in that

the South Australian form has a displaced

seoandary peak at L, = 0.08 ta 0.10 mm, L.,

= 4K 1 0.10 mm (Fig. 1k).

Coefficient of Thickening: Randomly selected

light andl dark laminue, and macroluminae.

were measured outside the crestal zone th),

then traced into the crestal vone and remen-

sured (H), H/h was plotted at intervals of

0.5, In a total of 52 measurements, the medal

value of Hh is the interval 2.0 to 2.5 (26.9% }

while only 15.5% exceed 3.5, and none less

than 1.0 occur (Fig. Ij),

Inierspaces; Interspave = Aillings — betweeir

colunms are strongly altered, consisting of

homogencous recrystallized Uolomite Seme is

of grumous texture, composed of xenotopic

equidimensional (0.005-0.01 mm) grains,

forming patches 0.05-0.10 mm in diam., set un

a §parry matrix of grain size 0.1-0.3 mm. The

only observed remnants of primary structure

are possible smull intraclasts in one specimen.

Secondary Alteration; Fracturing of laminae

is restricted almost entirely to the crestul zones

of some specimens and marginal zones ol

others. Portions of the crestal zone are more

or less breccated and recemented in place

(Fig tid). Contertion frequently occurs

within the crestal zane, Immediately outside i,

laminae wre deflesed: this and the brecciution

ate effects prubably due to compaction during

burial, The breeeiation of macroluminac into

cleanly broken fragments several imillimetres

long suggests that the carbanate was already

lithified during the deformation (Fig. 11d). Im

places, on the column margins, Jaminae

truncate underlying laminae. Whether this is

due to peneconiemporuneous crosion or ta

sliding of the overlying Jaminue during con-

paction could not be determined, but associa-

led brecciation around the colunm margin

sugeests the latter possibility. No overfolds or

diapirie structures as in Conoplyron gargani-

cum australe Walter (1972) were observed,

supporting the idea that columns were lithifted

soon after growth.

Columns and interspaces consist entirely of

dolomite. ‘The preservation of very fine lamina-

tion suggests that dolomitizuliun was probably

penecontempoerancous, All laminae are more

or less recrystallized, the dark laminac are

coarser and more transparent that ty the Rus-

sian or Western Australian forms. Recrystal-

lization may be due to the lew grade regional

melamorphism which has wffecicd the Mt,

Lofty-Olary Are. Pale laminae between dark

mucrolaminue are preferentialhy recrystallized,

emphasizing the distinctness of the macro-

laminue, These recrystallized lansinwe consist

of sparry. hypidiviopic 19 xenotepic incqui-

uniqular dolomite, of grain size UA2-0.10 mm.

The most recrystallized specimen is a fine

marble. in which dark macroluminac, approxt-

mutely 1 mm thick, contain no preserved in-

ternal lamimac. and consist of xenotopic equi-

dimensional curhonate with interlohbate crystal

boundaries, of grain sizes 0.02-0.05 mm. The

grain. size uf the light laminae is (450.10

min, und in places much coarser, One speci-

Men is extensively sillcthed. Silicification pust-

SOUTH AUSTRALIAN STROMATOLILES I! 95

dates the prowth of the whole column, and

may be related to tectonics and diapiric em-

placement rather thun to sedimentation, Silica

consists of xehotopic quartz aggregates, of

grain size 0.05-0,10 mm, in places containing

small dolomite rthombs. Portions are com-

pletely redolomitized,

Comparisons:

Fhe conical Jamination with thickened

crestal zone, and the absence of branching dis-

ainguish this stromatolite from all groups ex-

cepl Conephyron. Tt diflers from most cono-

phytons in that the columns are not always

parallel, hue theif original growth orientation

is not clear. due to structural disturbance. On

microstructural features, it falls into the Carp-

plvios garvanicwn subgroup (Conophyion

gosanicum, C. miloradovicl, C. guuhitza, and

perhaps, ©. /aseliicuna Walter), The closely

allied C, miloradovict has more irregular and

lenueculur laminae. ©. basakicum Walter also

has very thin smooth continuous laminae, but

lacks (he distinctive Types Tt & LIL erestal zone.

The absence of numerous knotted lenses and

sharp swellings distinguishes it from the variecly

Co wirganicun nerdiciun:. On these feutures it

was assigned to Conophyieit cf. garganicus by

Glaessner er al. (1969).

The statistical study confirms the identifica-

tion as Cy garganicum garganicum, and distin-

guishes it clearly from C, gareanicion australe

Walter und C. earganicum nordicum, The

modes of thicknesses 1, and Ly. most closely

resemble C, gurganicum garganicum, especially

Ly (mode at 0,04 to 0,06 mm), while most

other conophytens have modes at mugh higher

values, C. garganicum nordicum has a modal

value of L, at O10 mm, and C. gargeretnt

ausirele Walter at about 0.08 ram. The ratio

L/L, ts the most distinctive character for

Conophyion garganicunt garganieuin. The

modal value is the interval 0.50 to 0.75, which

fulls within the broader peak of the Russian

form (0.50 to 1.00), but distinguishes it from

C. garganicum nordicum Komat, Raaben &

Semikhatov (mode 2.00) and from C. gur-

gunicum australe Walter (1.0 10 1.5), The co-

efficient of thickening is less distinciive: the

mode at 2,0 to 2.5 does not distinguish C. gar-

gonicum garganicupr, C, miiloradovic? and C.

eviindricum but excludes C, garganicui nor-

dicum and probably C. g. atesrrele.

Distribution: Lower Subsuite of the Yusmas-

takh Suite of the west and east slopes of the

Anabar Massif; the Kyutingdin, Arymas and

Webengdin Suites af the Olenek Uplift; the

Gonam Suite of the Uchur-Maya Region,

Ust’-sukharin Suite of Western Priver-

khoyan'ye, Mongoshiit Suite of the south-

eust part of the Eastern Sayan, Bul'bukhtin

Suite of the Baikalo-Patom Mountains, Sat-

kin Suite af the Southern Urals: in pre-upper

Burra Group sediments, Paratog Diapir, S.

Aust.

Age: Early and Middle Riphean: in S. Aust,

itas assumed to he early Adclaidcan-

Group GYMNOSOLEN Steinmann

Gynineselen Steinmann 1911: $8 Semi-

khatov 1962, 219. Krylov 1963: R4, Kamar

1966: 88. Krylov 1967; 346, Raaben 1969;

73 {in parti. Glacssner, Preiss & Walter

1969; LOST.

Type Fernt. Gyinitesalen eanisoyi Stein-

mann, from the Dolomitic Suite of Kanin

Peninsula; also widespread in the Southern

Urals, the Polyudey Mountuins, Kildin

Island, and Tien-Shan, USSR.

Diagnosis: Smooth to gently bumpy, swelling

amd constricting, Walled columns with frequent,

>-patallcl, often multiple branching, less fre-

quently slightly divergent branching,

Contear: Grrinesolen camsayi Steinmunn;

G. levis Krylov; G. furcunts Komur: G.

altus Semikhatovy, "“G confragesus” (in

part) Semikhatoy and G, asyminetricus

Raaben, Rauben (1969) has included part

of the group Minjaria Krylov in Gymno-

salen, chiefly on the basis of microstruc-

tutal similarity, but Krylov (1963) has

clearly distinguished Minjaria from Gym-

eesoler by its regular, subcylindrical

shape of columns, of constant diameter,

and selatively rare and simple branching.

Ape: Late Riphean,

Gymnosolen cf. ramsayi Sicinmann

FIGS, 2b-z, 3a-c, 9b, 10b, 12b,c, 134

Gyninesolen sp, Glaessnet, Preiss &

Walter, 1969: 1057.

Material: Five spegimens from nears Wilsan

Description

Mode af Occurrence: All specimens ate bould-

ers from conglomerate and breccia bedks within

the Tapley Hill Formation on the flank of a

small diapir, Only one specimen shows com-

pletely separate, discrete, vertical columns, and

is interpreted to have been derived from the

central portion of a bioherm (Fig, 13a}, OF

two specitens showing much coalescing and

bridging. ome alsa has markedly inclined

columns (Kip. 12c). These ate considered to

96 W. V. PREISS

represent the marginal portions of biohernis.

The provenance of the boulders has not been

determined.

Column Shape and Arrangement, Columns

straight lo gently. curved, erect, 1-5 em diam.,

with gentle swellings and constrictions (Fig.

2b-g). Transverse sections generally circular

to oval, but lobate and rounded-polygonal at

branches (c.g. Fig. 3a). Length of columns

hetween branches 5-20 cm. Sone columns

short (only 2-5 cm long), with rounded or

pointed terminations (Fig. 2c.e). Colunins pre-

sumed to be marginal in bioherms are inclined

(as inferred Irom the asymmetry of Jaminac

and occasional interspace Jumination). “lhe

gross morphology of marginal colunins differs

only in their frequent coalescing und bridging.

und narrow interspaces (Fig. 3b). One speci-

men with appurently erect columns is markedly

humpy (Fig, 2d).

Branching: Slightly divergent to @- or. most

commonly, y-parallel. The column expands

SA. Déeparrmenr af Mines

Fig. 2. (a)—Conophyton garganicum garganicum, from dolomite raft in Paratoa Diapir. Part of a

farge column illustrating margin structure. $528: (b) to (g)—Gyrnasalen cf, ramsayi, from

boulders in a conglomerate in the Tapley Hill Formation, near Wilson; (h), {c), (e), GF).

(g)—Vertical columns interpreted to be derived from a binherm centre. S388: (d)—Poorly

presetyed vertical columns. $390,

SOUTH AUSTRALIAN STROMATOLITES "?

rapidly, then branches suddenly into two, three

or four columns, some branches lerminaling

as pointed projections. Even in the disercte

specimens, adjacent columns muy vecusionally

coilesce. The inclined-column specimens

branch similarly, hut widening of a columo

before branching js more marked. In these

specimens adjacent hranches either are [re-

quently linked by massive bridges, or coulesce

Margin Stevervre: The surface of columns

beurs low, rounded bumps, 1 to 2 cm wide.

with a reliet of « few millimetres, Short, trans-

verse Ur inclined tihs ure exceptional, Mostly

it is covered by a wall, up to 3 mm thick, com»

pasd af from one or two to ten laminac

(Pig. 12h. cb. Generally, the marginal zone

of columns is recrystullized, but in places, la-

minue bend down near the column margin and

extend parallel to it [nr up to 2 em. Leven

where wall reerystallized. outer lamina sharp,

well preserved, In places, an tnlaminated sel-

vupe, up to 0.5 mm thick. lines the column

surface. This post-chites the wall formation,

and pre-dates the interspace sediment. In the

dixerete column specimen. bridges rare: ocesn-

sionally where two columns are closely spaced,

afew laminae may bridge ucross. Rarely, over-

hanging peaks occur: especially iF draped over

gn adjacent intractast: some columns arise

from laminae grown over intraclasts. Columns

in the inferred marginal specimens purtly un-

walled: Jaminae thin and wedge out, forming a

amuoth murgin, but do not-extend over il.

Lusaina Shape: Varies within broad limits.

Gently convex laminae most frequent. varving

in sectiod from rectangular to hemispherical,

Frequently, laminae develup two oor more

crests pror to branching, but in some cases,

incipient branches are immuuately bridped

aver. und growth of the original coJumn re-

sumed (eg. the column on the right of the

photovraph in Fig. 12b). Different lamina

shupes. occur close together in w column, ie.

degree ol inheritance of shape is low. Fig. 96

illustrates commonly occurring shapes. OF li-

minye measured, 694% have h/d Tatio between

0.2 and 6,6, the mode (26%) being the inter-

vil helween 0.2 and 0.3 (Rig. 10b), (In deter-

mining lamina shape, the poorly visible, down-

turned marginal portions of Jaminac in the

will had to be excluded). Laminae mostly

slightly wavy, with wavelength 2 or 3. mm, and

amplitude 0.2-0.5 mm.

Micrasructure: Micrositucture extensively re-

ervstallized. Where alteration minimal, alter-

uating light and dark laminue of greatly vaty-

ing thickness form w distiner streaky miero-

structure ¢Fig. |2b). Lighr Jominue are l—

0.5 mm thick Occasional thicker livht laninae

(up to | mm) may actually be peervstallized

macrolumingae, Light laminae are ¢ontinious

ucross the coluron. but thin in the wall zone

Very rarely, they are ceuticated hy micro-

unconformitivs. They are wrinkled and wavy,

corresponding to irregularities in the Wark ta-

mite. und consist of sparry, cquidimensional.

xenotopic to hypidiotopic calcite, of grain sive

UAH-O.0S fom. Trregular patches, approsi-

mately 0,05 mm diam, are stuned With a pate

brownish (organic?) pigment. Dark lena

are 0,050.3 mim thick, hut pinch und swell

rapidly along their length. In many places, they

are lenticular, consisting of contiguous lenses

or nodules 0.1-O.5 mm fang. Usually dart

laminae persist ucrass the column, but occa-

sionally Jens gut completely. so thit adjacent

light laminae merge, The clirk laminae which

ure thickest in their crests. consist of brown

pigmented xXenotopic, cauidimensional calcite,

of wrain sree O.005-U.0ES mim. In places, dark

Jaminac limonitic. In arcas of more pervasive

recrystallization, prumous textures ie deve-

loped in Which clotty remnants of dark Liminae

are set in a matrix Of sparry hypihiotopic cal-

cite. Poorly differentiated macrolaminue, 0.5-

200 mm thick, consisting of up lo & light

dark Jamination pairs, occur in many purts of

columns, The internal structure of these 1s

often not preserved, resulting in more or less

homogeneous thick dark lammae with wavy,

sharp, upper surfaces.

/nterspaces 2 mm—5S.em wide: where colunms

more widely spaced, interspaces Filled with silty

intrami¢rite. Intfachiuts are flat pebbles [5-3

em long (Figs, 12b, c; 134, suhrounded, vari

ously oriented. und foosely packed (matrix

supported), Many stand vertically in the inter

spice. Some intruclasts are curved, suggestive

of a mud-cracked origin, The matrix consists.

of broadly laminated silty, recrystallized lime

mud) fine Jaminaé, 2-5 mm thick, consist of

yenolopic calcite of grain size 0,003-0,01 mim,

while coarse faminac, of about the same thick-

ness, consist of hypictotapie 0.03-0.05 mm

frain size calcite, with much subangutar quartz,

sill, Laminations of the interspace sediment

ubut against the column walls, having accu-

mulated after the development of significant

relief of columns,

Secondary Alrerution: laminae are extensivety

altered especiully ut the marginal wall zone.

In places the lamination is completely disrupted

OB Ww. V. PREISS

ufound centres of reerystallization, but cam-

monly faint lamination or sows of dark clots

ure preserved, to indicate the presence of ori-

ginully continuous dark laminae im the wall

vone, The outer few millimetres of columns

are ocommunly recrystallized to career,

twinned hypidiotopic calcite, of grain size up

to 0.3 mm with inclusions of dark lamination

relics, In places, am acicular texture is deve-

loped in the wall zone, perpendicular to the

column murgin. The central parts of columns

ure less affected, but even here, laminuc ure

commonly reduced ta dark clots in a sparry

culetre matrix. Dolomitization of both inter-

space and columns iy found in some specimens,

where anhedral to subhedral rbombs of dolo-

mite, 0.02-0.06 mim in grain size, are scat-

tered more or less uniformly throughout a re-

crystallized sparry calcite mosaic, Frequently,

lenses of coarsely crystalline, clear calcite

occur within the lamination. Coarsely sparry

patches, cutting gcross all earlier structures, are

probably infillings of solution cavities, since

they are closely associated with discordant

stylolites. Stylolites are rather rare, and of two

génerations, The first are concordant with la-

Minae, and contain concentrations of limonite.

These are cut by major calcite veins, which in

turn are offset by the discordant stylolites men-

tioned above.

Comparisons

The stromatalites ure assigned to Gynima-

salen on the basix of their column shape,

frequent y-parallel and slightly divergent

branching, and wall, In overall column shape

an Llype of branching, presence of pointed

projections, shape of laminae and micrestruc-

ture, (he South Australian form closely re-

sembles the type G, raniwayi. Slight differences

include unwalled patches. of columns, occa-

sional peaks and hridges, and in places it

slightly bompier margin structure, G. cf, ravn-

sayi as distinguished from G_ furcatis by the

absence of markedly y-parallel, multiple

branching and by the presence of pointed pro-

jections, and from G. levis by its more widely

spaced, Icss markedly bumpy columns, G. wits

Semikhatov has apparently been affected hy uw

strong cleavage, and its columns are slightly

deformed, making comparisons difficult, but it

appears to have a more continuous, banded

lamination. G. aywinmetricus Raaben has thin-

ner, smoother laminae thin G. ramsayi. G.

confragoxus Semikhutov has in part (specimens

from the Shorikhin Suite) deen reassigned by

Raaben (1969) to Inzeria Ul. confraeosa);

ese specimens are distinguished from G

ranisayl by their irregular columns, interrupted

will and more frequent peaky and cornices.

Semikhatoy's specimens from the Dashkin

Suste, now considered as Vendian (Krylov i

Rozanoy er af. 1969, p. 215), have much

smaller, bumpier columns than G. retmuseeyi.

Distribution; Sub-Inzer Beds of the Katay

Suite und Minjar Suite of the Karatau Series

of the Southern Urals: Niz’ven Suite of the

Polyudov Mountains: Carbonate Beds of the

Metamorphic Series of the Kunin Peninsula:

Kil'din Series of Kil'din Island; possihly the

Spatagmites af Norway; Bystrin Suire of

Southern Timan; Chatkaragai Suite af ‘Ten-

Shan: as clasts in Tapley Hill Formation. &

km E of Wilson, southern Flinders Runes.

S$, Aust.

Age: Late Riphean, in S. Aust,, not younger

than the Tapley Hill Formation.

Group INZERIA Krylov

Mngeria Kryloy 1963: 71. Krylov 1967;

29. Cloud & Semikhatov 1969; 1042.

Ravben 1969: 77, Glaessner, Preiss &

Walter 1969: 1057.

Type Form: Inzerid tianusi Krylov, from

the Katuv Suite of the southern Urals,

and the Demin Suite of the Polyuday

Mountains, USSR,

Diagnosis: Subparalicl, usually wnwalled, sub-

cylindncal, ribbed columns, frequently with

niches containimg projections Branching

mostly a- to @-parallel to slightly divergent.

rarely y-parallel or markedly divergent.

Conn: Lf. gomasi Krylov, £, toctagnlli

Krylov, f. intia Walter, and probably /,

djejimi Riaben and fF, ayfryslandica

Raaben, 4 (Minjarvia) nimbifera Semi-

khatov may he included, but Raaben

{1969u) has placed at in synonymy with

i. fjomusi, and has partly reassigned

Gynmosolen canfrayosus —Semikhatov

ta Snzeria (L eonfragoxa), Raaben haus,

however, considerahly broadencd the con-

cept of J/rseria, placing lille importance

on Krylev’s (1963) critema of ribbed

columns with niche-projectiony, On this

basis, Aldania Kryloy (ia Rozanov e¢¢ ol,

1969) could perhaps be better included in

fnzeria. Descriptions of 2. macula, 0.

varinsata, J, sevintedr and J. chunitbergiva

Golovanov were unavailable, but Raahen’s

(1969, Fig. 2L) illustration of frzerie

nrteuld docs not resemble any other des-

eribed J/nzeria. The new S. Alist, forms

are I, multiplex und |, conjpimera,

SOUTH AUSTRALIAN STROMATOLITES iL ed

Age and Distribution: \ate Riphean, wide-

spread in the USSR: Bellon Springs. Forma-

tion. Central Aust.; Brighton Limestone and

Wundowie Limestone, S, Aust; Hinde Dolo-

mite. and doubtfully, Dook Creek Forma-

lun, NT,

Inzeria cf. tjomusi Krylov

FIGS, 3h. 2, tieg, |3b-

Material: Three specimens from Burr Well.

Description

Made of Occurrence: “Vhe stromatolites form

a lenticular bed, interbedded in green shales,

and consist of fottr or five contiguous gently

damed bjioherms (Fig, (3c), 2-+ m diam,

with a inuximum thickness of about $ mi. Toe

wirds the west, the bed thins and lenses nut

grsdually; in the easterly extension, columiar

stromatolites give way to flat-laminated lime-

stone. The lower partion of a domed bioherm

consists of Hat-laminuted stromatolitic lime-

slone. or contiguous, very broad cummuly (part

of which are seen in Fig. 13d). up to 20 em

thick; overlying this (hut never seen in sedi-

mentary contuct with it), is a zonc, up to 20

em thick, of discrete, verticul, subcylindrical

eolurons, 2-10 em Wide, The base of these

columms is an intensely stylolitic zone, in which

aw thickness of up to several centimetres has

been removed by solution (Figs. 13b, d). At

the maruins uf bioherms, the columns become

inregular and slightly inclined from’ vertical.

Columns jre bridped over hy a thin, poorly

exposed zone of flat-laminated stromatolites.

Column Stupe and Arrangenenrs; Columns

short, subeylindrical, with some swellings and

constrictions, of diameter 2-10 cm (Figs, 3f. 2.

4a-g), henght 10-20 cnt (the whole thickness

of the columnar zone}, Transverse sections

round, rounded polygonal or slightly lobate.

Columns have vertical, straight axes in the

central parts. of bioherms, hut hecome irregular

at the edges.

Branching into discrete new columns rare, per-

haps due to the small thickness of the bed.

Niche-projections very frequent; they are short,

narrow, usually rounded, sonelimes xlighthy

elongated, set into niches in the side of the

tain column, which, most commonly. resumes

its former diameter at the top of the niche

4Figs. 13b, e: du, d, & g). Occasionally auja-

cent columns coalesce,

Margin Structure; Due to strong recrystiliza-

ton of columns the margin structure is ob-

secure. Laminue upproach the margin al u high

angle. and are not defiecxed at their cdges;

columns always unwalled. Lateral surface of

columns with numerous short transverse vibs,

up to 2 cm long, occysinnyl overhanging la-

ininue and peaks. Th places, adjucent columns

linked by bridges up to 5 mm thick,

Luminae Shape: Always genlly conver, vary-

ing in shape from continueusly curved domes

la very low, obtuse cones. as illustewted in Fig.

9c. Lamina shape inherited from underlying

Jaminae. without fapid chynves in convexity.

Ratios of h/d usvally low; 91% of laminae

huve h/d between 0.7 to 0.4 (Pig. 10e). Fine-

seule structure of laminae smooth to gently

wrinkled.

Microstructure: Strongly recrystallized through-

out columns, but in places the gross indistinctly

banded structure of laminae ts moderately well

preserved (Fig, 13e). Relatively thicker light

Jaminaé alternate with thinner datk laminae

hut recrystallization has in places obliterated

the distinction. All laminue have diffuse baun-

daties, Light laminae 0.2-2.5 mm thick, com-

monty significantly thicker al their crests than

their edges. especially in the obtusely-conical

laminae. ‘They consist of @ sparry, equigtanu-

Jar, hypidiotopic mosaic of calcite, of grain

size OES—O.02 mm, with ingluded small, irre

gular patches of darker pigmentation. Derk

laminae githee smooth or finely wrinkted

(largely due to embayment by recrystallized

adjacent light laminae), thickness 0,2-1.0 mm,

generally thinner than adjacent laminue. Oeca-

sional thinner dark laminae are lenticular, but

whether this feature is primury or due to Te-

erystallization is unresolved, Like the light In-

minae, they are slightly thickened in eheir

crests. Dark laminae consist of xenotopic,

slightly inequigranular calcite, grain size 0.005-

0.09 mm, stained with a pale brownish pig-

ment.

Interspaces filled with homogeneous recrystal-

lized lime mud, with occasional intraclasts,

Culcite xenotopic to hypidiotopic, grain size

0,01-0.03 mm, contains about 5% angular

quartz silt, Quariz grains corroded by recrys-

tallized calcite. Occasional flat intraclasts up to

1 cm long, with diffuse boundaries, in parts

of interspaces, recrystallized to sparry calcite

mosaic, prain size 0.02-0.03 mm-

Secondary Alteration: The whole reck is per-

vasively altered, While columns are pale grey,

tunsparent in thin section (Fig, 3c). the dark

laminae perhaps tinted with arganic milter,

iterspaces are pale buff probably due to the

presence of small amounts of limonile, Neither

columns nor interspaces are dolomitized, The

100 W. V. PREESS

S.A DérartmaAns of mines

FIG. 3

SOUTH AUSTRALIAN STROMATOLITES UI IU}

boundary between interspace and column is

always diffuse, obliterated by recrystullization

in both, This reduces the reliability of the re-

constructions. Highly irregular styloliles with

large Jubes sepatale the basal laminated sedi-

ment from the discrete columns, with a gone

up to 5 cm thick of intense brecciation and

late-sisge infilling of fractures by coarsely

ervstalline calcite. Possible remnants of the

lower portions of columns, highly enriched in

limonite, are sometimes preserved between

cross-cutting stylolites (Fig. 13e), Large sub-

aphericul nodules, up to 3 cm diam., of

coarsely crystalline culcite are very commun

in the litnestone at this locality. mostly located

withm columns, Twinned calcite crystals in

these highly elongated, 1-3 mm wide, up to

3 om long, vertical or radially arranged. Mast

crystals terminated upwards; their acute tere

minations project into the laminated limestone

of columns, The major cross-cutting stylolites

post-date the coarsely crystalline nodules. Qver

large areas, columns are completely tecrystal-

lized so that lamination is partly or totally ebli-

terated, Such areas consist of xenotepic, to

hypidiolopie mosaic calcite, gtain size up to

OS mm. Where rtecrystallization incomplete,

regular fragments of disvapted dark laminae

surrounded by sparry, recrystallized mosaic

calcite.

Caniparisons

The presence of ribbed columns with nu-

merous niche-projections places the stromato-

-lites in the group Inzeria, They are differen-

tiated from all other Australian forms of

fazerla and from /. rocrogulii Krylov and &

djejimi Raaben by their very infrequent

branching, consistently gently convex laminae

(grading to low-conical rather than reclangu-

far}, and their short Jength of columns. In hav-

ing subeylinerical, erect, mbhed columns with

nunverous niche-projections, they closely te-

semble Russian specimens of /, tjorud Krvlov,

hut differ in the thinness of the zone of

columns; the dbsence of branching may simply

be a consequence of the short length of

columns, Unlike 7, tjeaiuest [rom the Southern

Urals, steeply convex laminae arc absent. The

microstructure with pinching and swelling or

wrinkled dark laminae is similar, but the pro-

minent concentrations of iron oxides along

Fig,

concordant solution surfaces are ahsent. Until

bicherms are found in which the columns had

the opportunity to grow to 4 greater height,

so that the mode and frequency of branching

can be determined, and which are less recrys-

tallized. so as to preserve the margin structure.

no reliable identification ts possible,

Distribution: Middle limestone band of the

Wundowie Limestone Member, Umberatuna

Group: Burr Well, northern Flinders

Ranges, 8. Aust.

Age: Late Adelaidean, correlated with the

Late Riphean or Wendian of the USSR,

fnzeria conjuncta £. nov.

FIGS. 4h-m, 9d, 10d. 144, b

Muterial: Three specimens from near Depot

Creek.

Holotype: S402 (Figs. 4a, b, tj, 14a), from

the Brighton Limestone equivalent, 3 km

north of Depot Flat H.S., southern Flinders

Ranges, 8, Aust,

Neme: Latin cenjurea, meaning joined,

refers to the frequent coalescing and bridg-

ing of columns,

Diagnosis: Inzeria with broad, unwalled, rarely

branching, frequently bridged und coalescing

basal columns, which divide by «-parallel

branching into narrower, unwalled upper

columns with occasional e- and -parallel

brinches, Niche-projections moderutely fre-

quent, Laminae nearly flat to rectangular or

gently convex, wavy or wrinkled, with a dis-

tinct streaky microstructure.

Deseriplion

Made of Oeveurrence: Fiekd examination of

bioherms is hampered by the very extensive

lichen cover on rock, faces and by the discon-

tinuous outcrop. Three domed bioherms, up

to 50 m long, 3 m thick, occur interbedded in

massive oohtic and intraclastic limestone, and

cannot readily be differentiated from Acaciella

augusta in the field, The basal, central portion

of bioherms consists of flat-laminated stroma-

tolitic limestone, passing up gradationally into

bread columns, 5-20 em wide with frequent

coulescing und massive bridges. Flat-laminated

intervals may. intervene, At slightly different

levels, the broad columns divide by a-parallel

branching into 1-5 em wide columns.

3. (a) to fe)--—Gymiasolen cf. ramyay: from near Wilson, (&#)—S388, vertical columns pro-

bably fron: a bidherm centre; (b) and (d)—S387, inclined columns interpreted to be derived

from iw bioherm margin; (¢)—S389; (¢)—S390, irregular and frequently coalescing columns,

Traced from slabs; (f} and (g)—Jnereria ef. tienes’. Wundowie Limestone Member, Burr

Well, northern Flinders Ranges. $479.

102 W. ¥. PREISS

S.A, Department pf Miaies

Fig. 4. (a) ta (g)—lnzeria cf. umuasi, Wundowie Limestone Member, Burr Well, Northern Flinders

Ranges. (a). (b) and (cy, $5942; (d). (f£), and (2)—S480: (c)—S479: (fh) to Gin)—lazeria

conjuncte, Brighton Limestone equivalent, Depot Creek; (h), (i), and (j)—Holotype $402,

broad basal columns branching into narrow colunms; (k)—S403; elangate columns from a

bioherm margin; (1) and (m)—S398; narrow upper columns.

SOUTH AUSTRALIAN STROMATOLITES I

Caluma Shape und Arraigeneiu: Broad

columns in lower part of biuherms subeytin=

drical, up to 30 em high In their discrete por-

lions, comMronly with rounded polygunal trans-

verse sections, Where adjacent columns

coulesce, or a wider columm branches, transvetse

sections may be complesly lobate. Gverlying

narrow columns slightly clongated, from 1 x 2

cm ty 3 x 5 cm in transverse section, up to

15 cm long between branches. Columns within

central part of bioherm straight. erect (Fig. 4h,

i,j) while at margins, they become inclined at

45°. slightly curved and strongly elongated

(Figs. 4k, 14b), with swellings and constrice

\ions

franchiitg: Niche-projections are formed by

unequal, o-parallel branching, or, less com-

monly, divergent branching; the narrower

column is set into the niche in the main wide

column, Which generally resumes its former

diumetec after the termination of the projec-

lion, Where projections branch divergently,

they protrude beyond the margin of the main

column. Projections U.5=4 em tong. Within

hroad column level, branching (other than by

niche-projections) tare, Broad columns then

divide by a-parallel, rarely §-parallel branch-

ing, into narrower 1-5 cm wide columns,

which hranch again, less frequently, by o- or

#-parallel branching, In marginal zone of hio-

herm, branching #- to +-pafallel, often with

constriction at branching; niches stil] common,

but clongated parallel to the long axes of platy

colimns (Fig. 4k),

Margin Structure: Lateral surface uneven, with

very frequent. transverse ribs. same small pro-

jection’, bumps, bridges, und accasional small

peaks, Ribs, 0,5-1 cm wide. may be followed

around the column periphery for a few cenu-

metres. Both massive and delicate bridges accur

between adjacent colunins, and, sametimes,

between columns and projections, Niches in

the column margins 4 to several centinrebres

deep: some niches partly cloyed at one end

(Fig. 4h). Occasional niches clongated trans-

versely, grading into prominent ribs (Fig. 4h,

ji. There is no wall; at the column murgins,

laminae thin oanty slightly, and either end

abruptly or turn down and wedge out; they

do not envelop the lateral surface of the

column f{Fig. t4a).

Lamina sfape varices greatly from broad

columns to upper narrow columns. In broad

columns most laminae flat, geally convex, or

reclangular (Fig. 9d). In plices laminae deve-

lop to of more ¢rests, then either the column

103

branches (if near the branching level) or the

Interspuce is bridged over. and the column re-

sumes its normal growth (Fig. 14a}. In broad

columns, measured values of h/d ore below

O25. In the nyrrow, upper columns, laminae

ure Consistently more steeply convex. OF those

measured, 81% lic between 0,3 and 0.4, Col-

umns in the marginal zone of hioherms have

laminae strongly asymmetrical towards the ex-

terior of the bioherms, commonly as steeply

convex as in the upper narrow colamns ( 60%,

of h/d between 0.3 wml 0.4). Fig. Md illues-

trates the distribution of lamina convexites. All

laminac wavy, with wavelength 2—+ mm, and

locally wrinkled.

Microstructure distinctly streaky with butt

lenticular and continuous, wavy, swelling and

constricting laminae, Dark laminee O,05-0,3

mm thick, wrinkled and wavy, with non-paral-

lel upper and lower boundanes, sometimes

atading into aligned clots and lenses, They

consist of equigranular hypidielopie 10 idio-

topic dolomite, grain size 6.005-0.0L mm.

Crystals equidimensional and stained a pale

green lint, responsible for thé green colour of

the luminue. No individual grains of pigment

could be resolved even at 1200 x magnifica-

tion. Amplitude of waves and wrinkles 0.2-0.5

rom, wnd thickness of Iaminae changes rapidly

within a few millimetres. Ligh leniinae consist

of white to pale grey parily dolomitized sparry

calcite of axenotopic to hypidiotopic texture,

grain size 0.005—0,035 mm, tending to lens out

near column murging where adjacent dark

laminae merge. They also contain some coarser

detritus, including fing sund-sized, well rounded

quartz and feldspar, and small dolomite

thombs similar to those of the durk Jaminac

but less pigmented. Over most of the area of

thin sections, dark laminae tend to be grouped

into: macrolaminae 1-5 mm thick, which, like

individual laminae, pinch and swell murkedty-

There is evidence of minor contemporaneous

erosion of thickenings and waye-crests of

macrolaminze.

Interspaces; Both lower broad and upper uar-

row columns are separated by narrow inter-

spaces, 1-20 mm wide, but columns from bio-

herm mur'gins are almost in contact. The infill-

ing sediment ts layered, either by sandy lu-

Minac, or by single stromatolitic laminae

bridging between columns, Interspace laminae

ate depressed, concave upwards (Fig. 14n?.

‘The carbonate of interspsces is a dolemitized

limestone: slightly inequigranular hypidiotopic

calcite (partly recrystallized lime mud), grain

PREISS

WwW. Y.

104

SA, Depareoyern at tu

FIG. 5

SOUTH AUSTRALIAN STROMATOLITFS I

size 0.005-0.02 mm, contains subhedrul

rhombs of dolamite, 0.005-0.05 mm diam, In

places, quartz sand laminoe up to a few mil-

limetres Thick abut against the column margins,

suggesting that they postdate the growth of

that portion of the adjacent column. No cur-

bonale allochems were observed Av times of

bridging, the structures had a relief of less than

une centimetre, und bridging laminae may be

only one or two centimetres apart.

Secondary Alterqrion: Quartz and feldspar

erains, oth in columns and interspace sedi-

ment, have corroded bounduries; in pluces their

margins ate completely replaced by carban-

ate. While the dark laminae ure almost coms

pletely dolomitized, the lime mud comprising

the light laminae and the interspace filling is

only patchily dolomitized and also contains

hypidiotopic, coarser culcite due 1 partial re-

crystallization. The dolomitization is probably

secondary. Stylolites rare cacept in the bioherm

margins, where they separate contiguous

columns, Smull vughs. up to 3 mm diam, filled

with course, twinned sparry calcite occasiooully

cut across the lamination. The origin of the

green coloration of dark Jaminae is not clear,

since no particles of pigment could be resolved:

the dolomite crystals themselves are tinted.

Sunuce oxidation during weathering cither

partly removes the colour, or depasils yellow-

brown. limanite in interspaces or along style-

lites.

Comparisons

The stvomatolites are difficult to distinguish

in the field tram Acuciella cuynsta Preiss, but

ure assigned le Jazeria on the following charac-

ters! ribbed lateral surface, absence of wall,

dominance of purallel branching, and niche-

projections, The upper narrow columns also

resemble Ketaviie and Kulparie but are dis-

tinguished by the presence of long transverse

ribs, the absence of a wall. and by microstruc-

ture; unlike Katavia and Kulparia, their pro-

jeettons are usually rounded, und set in niches.

7. conjuncta differs fram 7, tlamusi Krylov and

/. mie Walter in having frequently coalescing

columns, and consistently genily conver, wavy

and wrinkled laminue; it lacks the consistently

elongated niche-projections and the complex

bioherms of /. intia. Unlike I. djejiri Raaben,

its columins are straight, with frequent niche-

Ins

projections, and rarer branching. J. conjuttcte

is distinguished from /. toctogulii Krylov by

ily less frequent, dominantly o-parallet branch,

ing, and by its coalescing and bridging, J. con-

juncta is especially similar to Aldania sibirica

in margin structure and mictustructure, but

has more irregular and coalescing columbss. As

pointed out above, A/dania night he hetter

included in Jazeria.

Distribution: Brighton Limestone equivalent,

3 km north of Depot Flat H.S.. southern

Flinders Ranges, S. Aust

Age: Late Adelaidean, correlfted with the

Yate Riphean of the USSR.

Inzeria multiplex f. nov,

FIGS. 5, Ge, 1Ne, 14c, d, Sy

Material: Six specimens froai figal Melrose

and Yednulue.

Holotype; S385, from the Brighton Lime-

stone equivalent, 8 km NW of Mt, Remark-

able, near Melrose, S, Aust. (Figs, Sa-i, 14,

d).

Name; Latin rudtiplex, meoning complex,

manifold or with many parts,

Diagnosly: Inzgeria with Trequent, dichotomous

to multiple, a- and A-parallel to slightly diver-

gent branching, and rarer branches arising

from niches, Columns have irregular transverse

sections. Margin bears ribs. bumps und shor

projections. Laminae gently convex, smanth to

wrinkled, with regularly streaky microstvuc-

ture.

Deseriprion

Made of Occurrence: Due to poor outcrop,

the exact mode of occurrence at Mt. Remark-

able is not known; a kirge bioherm is inferred,

since, when followed along strike, the stroma-

tolitic bed passes into massive intraclastic

limestone, but the contact is not exposed, Al

Yednalue, the stromatolites form a very thick

bed, which has not been waced Juterally. In

outcrop, the stromatolites at Mt, Remarkable

resemble literally linked forms, and columns

becoine discernible only when the rock surface

1s Cut.

Column Shape and Arrangement, Colunnis

tuberous to subeylindrical, erect to inclined

(Figs. 5; 14c, d), with steaight or gently curved

axes: Occasional columns sharply bent, espec-

tally when ussoci:ted with coalescing, Height

Fig,

*, (a) to ())—fazeria multiple, Brighton Limestone equivalent, southern Minders Ranges:

(a-i)—Holotype $385, west of Mount Remarkable: ¢j, k}—S499. Flogt specimen, east of

Yednalue, (1, m)—S498_ Outcrop specimens, cast of Yednalue.

hits Ww.

of columns between branching 4-21) emt, Trans-

verse sections of columns round or rounded

polygonal to irregular and lobate at points of

branehing or coulescing. Columns which may

be variously clongated, vary From 1 lo 5 em

in diam. AL top of bed, columns frequently

bridged by continuous, laterally linked layers.

Branching very frequent and complex, either

arising (fom niches in the parent column

{Fig. Si). or, most commonly, by equal divi-

sion (Mig. 5a, b, ¢), usually 2-parallel. rarely

u- OF y-parallel, or slightly divergent (Figs. 14c,

H5a). Adjacent columns frequently coalesce,

especially in the upper part of bed,

Marein Srructare; Column margin’ irregular,

with numerous, short transverse ribs, low

bumps and some Slizhily overhanging laminac.

Bumps and ribs tocally grade into yery short,

outgrowing projections, less than 1 cm long,

which are more common than projections set.

in niches, especially in the Mt. Remarkable

specimens (Pig, 14d). There is no wall; com-

monly gently convex laminae terminate at the

column margin, without bending over, some-

times overhanging to form sniall peaks and

cornices. Small pertions of column margins

relatively smooth. Bridges involving any num-

ber of laminae are common, especiully near top

of bec.

Lanning Shape: Almost ulways gently convex

(Fig, 9e}) even in the narrowest columns h/d

docs nut exeeed 0,5, Ol laminae measured,

93% have h/d between 0.1 and 0.4, the made

(40%) being in the range between U2 and

0.4 (Rig. Tey. Larminac may be dayhbly-

crested, prior to branching, On a small-scale,

laminag brondly wavy, and in places slightly

wrinkled,

Microsiructure: Alternalion of light, sparry

laminae and dark, iron-stained laminae, with

indistinct boundaries and varying continuity.

In places, laminae grouped into macrolaminae

1 or 2mm thick. Boundaries between laminac

frequently wrinkled. Light laminae (0.1-1.5

mm thick, usuilly constant weross the column

width, smooth, wrinkled or wavy (Fig, 14c),

with parallel wpper ynd lower boundaries.

Varying abundances of fine: quartz sand and

silt are incorporated in the light laminae, which

consist of hypidiotopic to idiotopic carbonale.

erain size 0.01-0,03 mm. Grains equidimen-

sional, sometimes cuhedral. Dark laminae

thinner, generally 0,1-0.5 mm, but pinch and

swell geross the column width; crests wl

laminae commonly thickesi Dark taminac

V. PREISS

erade [ron smooth fo wrinkled, and frequently

become discontinuous, forming chains of clote

and lenses up to 1 mm long, separated hy

sparry carbonate (Fig. I4c), Dark laminac.,

clots and Jensex composed of reddish-brown

iron-stained, xXenotopic carbonate, grain size

0.003--1.01 am,

liiterspaces: Columns gencrally closely spaced,

interspace width 1 mm-—* cm, The sediment es

different in the two areas of occurrence.

t1)At Mt. Remarkable, if is broadly lamnu-

leU redilish dolomicrile; laminuc 1— mm thick.

generally fist or slightly concave upwards

Darker laminae generally thinner (up te |

mm), of xenotepic dolontite of yrain size

O.N03-—0,005 mm, alternating with thicker,

paler, laminue, up to 4 mm thick, of xenotepic

dolomile, 0,005-0.015 mm grain size, with a

high pereentuge of terrigenous detritus. [angu-

lar ynartz silt of grain size 0,02-0.05 mot,

und occusionu) micu flakes). Intraclasls up to

T cm Jong, 2 mm thick, locally present in

interspace. generally siunding vertically or in-

clined (Figs. l4e, d).

(2) At Yednalue, the interspaces are filled with

unlaminated sandy limestone, with quarts snd

feldspar grains, 0.1-1.0 mm grain size, sub-

rounded to well rounded, all embayed hv

hypidiotopic to idiotopic calcite cement of

grain size up to 0.6 mm, Sand grains mostly

tightly packed, in places separated by a green-

ish argillaceous matrix (Big. 15a).

Secondary Alteration, Specimens from Mt.

Remarkable consist entirely of dolomite, while

those from Yednalue are calcite. Mt. Remark-

able specimens are, however, better preserved:

the idiotopic and hypidiotopic dolomite pro-

bably formed during early diagencsis, but did

not destroy the fine structure of the stroma-

lolites. The dolomitic rock may have proved

Mare resistant to later recrystallizalion, which

has in both areas disrupted the fine damination

to a greater or lesser extent, In adthtion,

cleavage is well developed at Yednalue, and

the columns are slightly deformed, sa thit

metamorphism may partly account for the

greater reerystallization here, Occasianal con-

cordant slightly sutured stylolites follow the

lamination, sometimes affecting xeveral adja-

cent colunins, but all are cross-cutting ono fine

scale. Greenish orgillaceous matenal is con-

centrated in the stylolites. Some stylolites fol-

low column margins and thus remove the

Minor surface features of columns (Fig. 15a).

Tectonic veins are filled with quartz or calcite.

SOUTH AUSTRALIAN

Compur/sans

The stfomatelites arc assigned to Ingerta

because of their ribbed columns with projes-

lions, but they frequently resemble Baicalia in

their tuberous shape; Baicd/ia, however. much

more ollen hus divergent branching, more over-

hanging lominae, and a distinctly banded

microstructure. In having some a-parallel

branching,, they resemble Kassiella Krylov

and Acacielle Walter, but are distinguished by

their Frequent f@-parullel branching and

branching from niches, Inzeria sueltiplex 1s

distinguished from f. rjomusi Krylov, 1 inva

Waller, and /. confined Preiss by its very fre-

quent branching. and rare projections set in

niches. In these features it resembles J, focfe-

eulti Krylov and J. djejind Raaben, but /. rocte-

euiit has more regular, cylindrical colunins,

while F. djenimi has steeply convex laminae.

Distribution: Brighton Limestane equivalent;

8 km NW of Mt. Remarkable and 12 km E

of Yednaluc, southern Flinders Ranges, S,

Aust.

Age; Late Adelaidean, corretited with the

Late Riphean of the USSR.

Group JLUIRUSANTA. Krylov

Jiirusenia Kervlev 1963; S81. Raaben

L964; 93, Krylov ir Rozanoy er af, 1969:

195. Cloud & Semikhatoy 1969: 1045-

Semikhatoy, Komar & Setebryakov 1970;

166. Bertrand-Sarfati 1972: 52.

Type Form: Jurisania cylindrica Krylov,

from the Katay Suite of the Southern

Urals.

Digenoasis; Even, — parallel, — subeylindrical

columns with round ot oval transverse sections

and tare, dichotumuus g-parallel branching.

Columns partly walled, partly bear downward

directed peaks and overhanging laminac, fre-

quently covered with an unlaminated selvige,

Conen Jurusania cylindrica Krylov, J,

tumuldurice Krylov, J. nisvensis Raaben

and J, judemicn Komar & Semikhatov. J,

shirica Jakoviey has been transferred by

Krylov (1969) to a new group, Aldana,

but Semikhatov, Komar & Serebryukov

(1970) retain ils assignment to Junesanni,

Bertrand-Sarfati (1972) has erceted new

forms J. derbalensis, J, lisse, J. alte,

Age: Late Riphean to Vendian,

Jurusania burrensis f. nov,

FIGS. Ga-l, YF 10f, 15b-, 16a

Miulertalt Four specimens trom Burr Well.

Hoefotype; S543 trom the upper limestone

SUROMATOLITES 1 17

band of the Wundowte Limestone Menrber.

Wirr Well, northern Flinders Ranges, 8.

Aust. (Figs. bd. ¢, f, 15e).

Name: After the Burr River, on the bank of

which the stromatolites occur.

Diagnosis; Jurusania with smooth to gently

bumpy, partly walled columns and local, short

peaks and overhanging laminae. Lamina shape

gently convex to subconical, laminae lenticular

with diffuse, streaky microstructure. Columns

puttly covered by an unlaminuted selvage.

Descripion

Mode of Oecurrence; The stromatolites occur

in lenticular beds af contiguous spherical and

subspherical bioherms up to 2 m diam. (Fig.

L5¢c). The bioherms consist of 3 concentrically

arranged zones. capped hy an undulating

columnar zone. Bioherm cores up to 50 cm

thick consist of irregularly pseudocolumoaur

and columnar-layered stromatolites of dark

grey limestone, overlying sandy limestone with

large, reworked intriclasts. Cores surrounded

by concentrically laminated zone, from whith

long straight, parallel columns arise. At bio-

herm margins, columns slightly inclined, rarely

subhorizontal: generally columns remain sub-

parallel throughout the bioherm, but show

more bridging and coalescing al. margins,

Spherical bicherms, mutually in contact. over-

lain by Mat or broadly undulating 1 m thick

beds of columns with numerous bridges and

pseudocolumns.

Column Shape and Arrangement. Coluinns

long. straight, purallel or radially arranged,

cylindrical or subeylindrical. In one specimen

from near the base of a bioherm, columns

somewhat inclined. irregular, tuberous, und of

strongly eblipuieul op Jobate transverse section

(Fig. Gb, c); otherwise transverse sections

round or slightly ellipticul. Columns mainly

smooth, with only occasional low, hroud bumps

(Figs. Ga-d, 15h, d, e); single columns gene-

rally have constant diameter, 5-10 em for basal

columns (Fig, 6h) und 2 em for upper, nar-

row columos (Fig. 6d, ¢, £), Length of columns

between branches nwy exceed 30 em; the

whole columnar zone of bioherms is up ta 1

mi thick, Columns in the overlying undulating:

bed rather short, and {frequently bridged, ap-

parently arising trom basal, flat-laminated

siromalolites (Figs. 6a, 6a, specimen S48.

but the exact location of this specimen in the

hioherin is not certain).

Branching cather infrequent especially in nar-

Tow, Upperthost columns, which may be up lo

108 W. V. PREISS

SA. Department st Mines

FIG. 6

SOUVH AUSTRALIAN STROMATOLILES 11

30 cm long between branches, but more often

terminate their growth befere branching,

Branching wlways dichotomous, either q-. or

slightly B-parallel (Figs. 6g, b), Occasionully

two neighbouring colunms miy cualesce, espe-

cially in upper parts of bioherms.

Margin Sirucinre geverally smooth, walled or

unwalled, bearing only hroad Jow bumps

several cm wide and of telicl up to 5 mm

(Figs. 6a-h), Lamjnic generally approach the

margin ul an acule aligle, but the actual margin

is Lrequently removed by stylolites. In areas not

aftecuod by stylolites. laminae either terminate

at mareii, or extend down for u distance of up

to |ocm to form a patchy wall (Fig. 15d, e).

{ns a few places, laminae overhang slightly to

form) small peaks, a lew mn long (Pig. Ge, f,

2), Larye overhanging peaks developed only

an the irregular columns (rig. Ob). from the

lower parts of bioherms. Considerable areas

ul smooth columns coated with a xclyage, 0.2-

1.0 mm thick. of unlaminuted very fine grated

culeite 1 Fig. 15d).

Lamina Shape varies to some catent with

column width, but most laminae gently convex

with relief about | cm (85% have h/d between

.2 and 0.5, Big, LOf): # Few narrow columns

haye <teeply convex to subconical Jaminac

(Fie. 9f). Laminae smoothly curved, micro-

unconformities rare, Laminy shape always in-

herited from the underlying laminae, so that

ho marked, tapid changes occur. Fine seule

structure of lamibue lenticular and very gently

wavy, with wavelength of 2-5 min, amplitude

Oo. mm

Microsimeivre: The dark limestone comprising

the pscudocolumnir bioherm cores is almost

entirely recrystallized, and even the lamination

is yarely preserved. Lamination in columnar

parts of hioherms diffuse, streaky, consisting of

altemating, finely wavy, lenticular, dolomitized

sparry pale laminae and darker, micritic

laminac, which intergrade. Micritic lanvnae te-

crystallized to microspar, grain size 0.005—

0.015 mm, of xenotopie, polygonal, equi-

granular texture: they have very vague boun-

daries, and vary in thickness from 0.2-0.5 mm

over short distances. Tn places, luminae thin

and terminate Jaterally, or consist of short,

Fig.

hut

ligned lenses. a few millimetres long. Sperry

laminae O.1-0.5 mm thick, pinching and swell-

ing but more continuous ucross colunin width,

consist of hypidiotopic to xenolopic calcite.

crain size 0.01-0.03 mm, with scattered sub-

hedral dolomite crystals, grain size 0.015-

0.06 mm. In places, laminae almost completcly

dolomitized, consisting of closely packed hypa-

diotopic dolomite with remnant interstitial

sparry calcile, Sparry laminae may nlso be

completely recrystallized, with little dolomitiza-

tion, to a hypidiotopic mosaic of grain size up

to 0.2 mm. The unlaminated selvage present

in places on cohinin margins consists of xeno-

topic calcite mosaic, grain size 0,005-0.02 mm;

its origin is not. clear (see secondary alteration),

fuerypuces: Columns 0,5-2.0 cm apart. Mter-

spaces filled with poorly bedded intramicrite.

partiwly dolomitized. Thtractasts smostly fiat

limestone pebbles, 0.5-3 mm thick, 2-30 mm

long, generally lying parallel to bedding, or

standing vertically in narrowest inierspaces

(Fig, 15d), The flat pebbles, which commonly

have rounded margins, consist of xenotopic,

eqyuigranulur mosaic eulcite of grain size up in

0.01 mm, and contain scattered subhedril dolo-

mite erystals, grain size O.0TO-0,.0L5 mim. Sub-

taunded to well rounded quartz ond Eeldspir

sand grains occur in places. Intraclasts mode-

rately loosely packed, so that some in contact.

some not; sediment was probably matrix-sup-

ported. The matrix. probably originally micti-

tic calcite, recrystallized 1o xenotopic inequi-

granular texture, grain size up to 0.015 mm,

oceysionally with scattered dolontite erystals.

The matrix, may he preferentially dolomitized,

Tn the specimen apparently fram the unitula-

ting bed capping hioherms, interspaces filled

with markedly upward concave laminated, re-

crystallized lime mud, without Intractasts; In-

minue somewhat thicker (approximately 3

mm) and more regular than those of the stro-

matolite columns.

Secondary Alteration: Kven thé finest calcite

laminae have probably undergone some recrys-

tallization to form 4 very Tine grained calcite

mosaic, Dolomitization apparently postdates

this, as subhedral dolomite crystals cut across

the calcile mosaic. In places, especially meal

fi. (a) to ¢h)—JSurusania brerensis, Wuodowie Limestone Meniber, Bure Well, nistthern Fit:

ders Ranges! (a)—S481; basal columns arising from wndulating stramatolites; (bj, foy—

S483: irregular columns at biohermy margin; (a), (2), (£)—Holotype $343; regular narrow

upper columns; (2), Ch

Brighton Limestone equivalent,

(h)—S482; regular broad, Jower eolurans: (i) to (o}—-Kytavia costata,

Depot Creek, southern Flinders Ranges: (7), G), (1). Gm).

in), (0) Holotype $175; narrow, subcylindvical eolurins; (k)—S519; basal columns arising

from undulating stramatolite,

114

column margins, liminae wre completely re-

constituled to mw coarse, Xenotopic. polyganal

calcite Mosaic. grain size up to 0.5 mm; these,

in turn, contain subhedral dolomite crystals. as

well us disrupted rermnants of mieritie laminne.

The origin of the unlamingted selvage is pot

Clear, wherever it was observed, laminae are

somewhat coarsely recrystyllized immediately

adjacent to it inside the coluiin, and the sel-

vage may simply be the outermost lamina of

the wall preserved from rectystallization, bul

this is not certain since the selvage is unla-

minated. and laminae cunnol usually be traced

directly into it. There ure at Ieast two genera-

tions of calcite veins: the earlier ones are more

imegular, finer grained, and contain dolomite

rhombs, suggesting that they pre-date at least

one period of dolomitization. The younger

veins are straight, more coarsely crystalline.

and post-date dolomitization. Dolernitization

in these stromiatolites is, ut least in part, very

late Giugenetic.

Coniparisons

In having long, straight, infreyuently

branching columns without rapid changes in

Uiameter, these stromatolites are distinguished

from idl but Minjariae Krylov and Surusania

Krylov, They are distinguished from other a-

or #-parsilel branching stromatolites (Boxenia

Korolyuk, deaciellt Walter and Katavia Kry-

lov) by their infrequency of branching. Min-

Jatia Krylov, however, has a ubiquitaus wall

und. lacks pedks and overhanging laminae,

Jurusaunia Keyloy may have either a patchy

Wall or no wall, pumcrous peaks, und [re-

quently a selvage covering columns, /. burren-

sis. is intermediate between Minjaria und Juru-

série Hut ass wssizmed tu the latter because of

its patchy wall and the presence of peaks...

hurrensis dillers Tram J. evlindrica Kryloy in

having a better developed wall, smaller and

fewer peaks, and less well defined lamination;

however. lamina shape is similar. J. deme

dunia Krylov is distinguished by its consistent,

well defined ribs and general ubsence of a wall,

J. burrensis 15 distinguished from J. nisvensiy

Raahen by its. inuch more even, smooth

columns which do not grade into or uhernate

with ps¢udocolumns and juterally linked

stromatolites; also, there ure no sharp changes

in limina shape as in the latter form, J, jude-

miei Kamar & Semikhatoy hus targer, often

strongly elongated columns, lacking a wall. J

derbalenis Bertrand-Sarfuti und J. alta Bers

tranw-Sorfari vlso lack wulls and have ragged

column ntargins, J, lisse Berttand-Sarfau is

W. V_ PRETSS

distinguished by the absence of peaks and cer-

niccs, and by more frequent branching,

Distributions Upper limestone band ot

Wundowic Limestone Member, Burr Well,

northern Flinders Ranges, S. Aust.

vtge; Late Adelaidean, correlyted with the

Late Riphean or Vendian of the USSR.

Group KATAVIA Kryloy

Karevir Krylay 1963: 94. Rauben 1969 83.

Glaessner, Pretss & Walter 1969: 1057.

Type Form: Katatia karatavica Krylov.

from the Katuv Suite of the Southern Urals.

Diagrens: Predominantly @-parallel branching

straight. subcylindrical, walled columns with a

markedly bumpy murgin structure.

Centent; Katavia keretaviea Krylov und

Katavia costata 1. nov.

Age: Late Riphean.

Katavia costata (, nov.

Katavia sp. nev.

Walter 1969; 1057.

FIGS. 6-0. 9g, (Oe Lob-d, 17u

Marerial: Seven specimens from near Depot

Creck, S. Aust.

Holotype: SUTS (Pips, 61, 1, myn. 0. beat)

from the Brighton Lintestone equivalent,

Depot Creek, southern Flinders Ranges. $.

Aust.

Nene: Latin costata, meaning “ribbed”,

refers (o the short ribs. present on the lateral

surface of columns.

Diagnosis; Katavia with very closely spaced

parallel columns, a thin wall, very indistiner

and wrinkled Jaminae. and a prominently

bumpy and ribbed margin structure with some

very short pointed projections,

Descriprion

Mode of Occorrenee: The stromatolites form

two Jenticular bioherms, 5m thick, and up te

100 m long. in the upper, pink dolomite mem-

ber of the Brighton Limestone equivalent. The

basal one metre consists of wrinkly flatelamina-

ted dolomite, with concordant atylolites. This

zone gives rise directly Ww narrow, parallel

columns (Fig, 6k), which continue through-

out the height of the bioherm (Pig. 16b). At

Frequent intervals columms cut by horivantsl,

concordant stylolites, The upper surfaces of

hioherms not exposed. At margins of bidherms

columns became inchned at »hout 45° (Fig.

17a), hut no horizontal columns were observe.

Colum Shape ane Acrungenent; Columns

long, straight, yerv closely spaced, diam. 05-3

Glaessner, Preiss &

SOUTH AUSTRALIAN STROMATOLITES I

cin, most commaniy 1-2 em (Fig. 16d). Most

columns vertical, except near bioherm mar-

gins, Cross-sectians round to polygonal, often

resembling iid-cracked polygons (Fig. 16c}.

Columns may be 5-20 em long between

branches: occasional columms only a few cm

long have pointed terminations (Figs, 61 J. 1.

m. n, ).

Branching moderately frequent, predominantly

-parallels a column 1.0-1,5 cm diam. widens

gradually to 2-3 em, then divides into two, less

often three, aurrower columns (1-1.5 ¢m in

diameter}, u-parillel branching from broad

colurnns does nat occur, Sone branching very

slightly divergent,

Murvitr Streedure: Lateral suctace of colunins

markedly bumpy and ribbed (Fig. 61-0}.

Fquidimensional bumps. 0.3-1,0 cent diam,,

with a relief of 2-5 mm most common, These

prade into |runsversely elongated ribs, which

partly surround the columns, Small. pointed

projections up ta | em long moderately fre-

quent (Pig. 6i, 1). and in places slight niches

in the column margin (Tig. 16d), Overhanging

peaks extremely rare; bridges absent in speci-

mens studied Near column nvrgin, laminae

4urn down steeply to cover lateral surface for

short distances, so that onty two or three la-

minge form the wall (Fig. 16d), which is deve-

laped almost everywhere, cuveriag all bumps,

Tibs jind projections.

Liwitece Shaper Laminge in basal, Mat-lamina-

jed portion poorly preserved, but appear Lo be

wivy and wrinkled. The lowest narrow

columns venerylly Have gently convex, wavy

and wrinkled lalinae, but degree of convesily

increases upwards, Undulations have wave-

lengih 2-5 1m. Fig. %¢ illustrates commonly

occuring famina shapes, 62% of laminae

measured have b/d hetween 0.3 und OS (Fig.

102), Most laminae hemispherical, some wp-

proach rectangular shape. Luminae near the

most hurpy column margins commonly

strongly wavy,

Micrastructere: Lamination in all specimens

extremely indistinct. Where best preserved, it

consists. of alternating relatively lighter and

darker, pale brownish stained dolomite Ja-

mings. many of the light laminae containing

uctrital quartz sand grains, restricted to the

central paris of columns. Liehd laminae have

extremely indistinct boundaries, are 0.3-2.0

mm thick, and thin myrkedly towards column

margins. Included sand grains subrounded to

subanvular, yrain size 0.05-0.5 om. Balomite

hypidiotopic, of inequidimensivnul erystals.

grain size 0.005-0,025 mm, often showing up-

proximate rhombic outlines, There are vatin-

tions in the intensity of the brownish pigmen-

Igtion present In the crystals, Dark lamilnee

extremely fine grained, more densely stained

teddish-hrown, O.05-0.5 mtn thick, most

clearly visible and thickest in marginal por-

lions of columns, but thin, markedly wrinkled,

unc discomlinucus, frequently consisting of

lenses only | or 2 mm long, in central part.

Towurds margin, dark laminae frequently

merge

Mnterspacey extremely niyrrow, 1-3 mm wide,

most commonly 1—2 mm. Sedinventury Alling

Unliminaied, comasis of equal propurtinns. of

sand and dolomite nratrix, Quartz sand grains

subrounded, cummonly 0,2-0.5 mm diam. a

few up to 2 mm. Feldspar and red. extremely

fine vrained, possibly igneous rock CLragments

sub-ordinatc, Matrix consists of hypidiotopic to

xenotopic dolomite, with equidimensional crys

tuls of grain size 0,005—0.03 mm, patchily re-

erystallized ta hypidtotepic sparry dolonite of

0.03.05 mm grain size. Intraclasts of pale

brownish fine grained dolomite, up ta 5 mm

fang. 2 mm wide occur in places mixed with

sand jrains. These probably represent frag-

mented alval laminie.

Secondary Alteration; The generally poorly

preserved microstructure of stromalolitic and

interspuce dolomite and its corrosion of quurlz

Brains suggest that it is secondary. Small irre

gular patches of recrystallized, fine sparry dolo-

mite arc scattered throughoul columns ans

interspaces. Layering in stramatolitic columns

is extremely tndistinct, and defined only by

slight vanations in grain size and pigmentation;

this general homogeneity may be partly duc to

dolomitization. Dark laminae are in places dis-

fupled, perhaps by recrystallization of the

intervening light laminae. All detrital quartz

grains have corroded margins, nsually sur

rounded by a thin tim of Jinely crystalline

spurry colomite. Authigenic chlorite is deve-

loped in places in the interspace sediment near

enlumo margins. Small stylolites are developed

locally near column margins bud are unimpor

lant, Prequent (urge stylolites, concordant with

bedding, were seen in the field (Fig. 173),

These we up ia 1 om wide. ond contain

marked concentrations of sand and auchiuenic

chlorite,

Comparisons

The stromatolites are assigned Lo the group

Ketavia becuuse of their A-parallel branching,

bampy, walled columns. They ine distinguished

92 W. V. PREISS

etl

5cm

—e

3.4 Depotment of Hines

Fig 7. (4) to (m)—Kulparia kulpurensiy, Etina Formation equivalent, near Kulpara, northern

Yorke Peninsula: (a). (6b), (c), (e), (i) —Holotype $380, frony unit C (Fig. 8}; (d), (m)

—S419; junctions between two contiguous domes, unit C (Fig. 8), (m) is cut by a sand

dyke, including stromatolitic fragments; (f), (g¢)—S420, from unit E (Fig. §)3 (h)—S271,

from unit C (Fig. &); (j)—S381, (k), ()—S270. from unit A (Fig. 8).

SOUTH AUSTRALIAN STROMATOLITES II i

from most other walled stromatolites by their

markedly bunypy murgin structure, and from

Patomla Krylov by their predominant simple,

B-parallel branching. Like the illustrations of

Katavia karatavica Krylov, K. cestata has. a

few very short pointed projections. It is ex-

tremely similar wo K, Acratavicu in tts gruss

form, micrustructure and margin structure, and

is distinguished only by ils. more closely spaced

columns and by the possession of short trans-

verse ribs,

Distribution: In two iioherms. upper (dolo-

mite) member of the Brighton Limestone

equivalent, 3 km N of Bepor Plat HL.S.,

southern Flinders Ranges, S. Aust.

Age; Lute Adeljidean, correlated with the

Late Ripheun of the USSR-

Group KULPARIA Preiss & Waller

(in Wulter 1972: 151)

Pulomia sp. nov., Glaessner, Preiss & Wal-

ter (1969, p, 1057).

Type Form: Kulparta hulparensis Preiss,

from the Etina Formation equivalent, Wm-

heratana Group; Yorke Peninsula. S. Aust.

Name: After the township of Kulpara,

northern Yorke Peninsula, &. Aust.

Diagnosis: Long, nearly straight, parallel

bumpy columns, erect or radially arranged

with very frequent coalescing and bridging,

moderately frequent u- and A-parallel branch-

ing and a wall between bridges: projections

may be moderately frequent,

Canrent: K. kulparensis Preiss and KR. aliete

(Cloud & Semikhatoy) Walter.

Comparisons

In gross form, Kidparia resembles Minjaria

Krylov und Boxenia Korolyuk, but is distin-

guished by its bumpy column margins with Fre-

quent bridging and ecovlescing, Like Natavia

Krylov and Paonia Keylov.. it has a walled,

bumpy margin structure; Katavia colinns

have /-parallel branching, no bridges and they

rarely coalesce, while Patontia hus frequen

slightly divergent branching and very nu-

merous pointed projections, Some illustrations

of Palomia ossice Krylov. from the Malokaroy

Suite, resemble AKudparia in having bunypy,

long subpurallel columns with fewer projec-

tiuns, but lack the frequent coulescing und

delicate bridges of Kulperia. Kulparia kul-

parensis was initially assigned to Patamia on

the busis of this similarity (Glaessner, Preiss

& Walter 1969). Kuloaria differs from Linefle

Krylov in lacking gnarled and tberous

columns, and trom Gywnesolen Steinmann in

lacking y-parallel branching. in gross forfn,

Rulperla alsa resembles the walled parts of

Inzeria intia Walter but is distinguished by the

absence of niches and elongated projections,

Distribution; Elina Formation equivalent,

S. Aust. and Bitter Springs Formation, €

Aust,

Ape! Adelaidean.

Kulparia kulparensis f. nov.

FIGS. 7, 8, 9h, LOh, 16e, b7b-f

Material: Eleven specimens trom Kulpara.

S. Aust.

Holeioype: S380 | Figs. Ja, b,c. & 1. 17d, a)

from the EBtina Formation equivalent, Kul-

para,

Name: After the township of Kulpara,

Diagnoyis: Kudparia with very frequent delicate

bridges, moderately frequent pointed projec-

tions und variable lumina shape, from gently to

steeply convex. Microstructure diffuse, irregu-

arly streak v.

Descriplion

Mode of Occurrence: A bed traced for at least

400 an, its noarthern extension not Known,

while its termination in the south can be lo-

cated only approximately, due to lack of expo-

sun. Strramatolitic bed up to 13 m_ thick,

occurs at passage from flaggy pale grey clean

limestane lu massive, grilly. cross-bedded

limestones, The basal portion of the bed (A)

(Fig. 8), commencing contormably upon the

fiagey limestones, consists of short, partly

divergently branching columns and psctudo-

columns, in thin beds up to L5 om thick, with

numerous bridges and continuous, nearly fat-

laminated layers. This is overlain by a broadly

domed biostrome (C) of long, narrow, vertical,

parallel, very closely spaced columns, arising

from a laterally linked zone and short, browd,

basal columns (B). ‘The upper surface of the

biestrome of long parallel columns hends

downwards sharply at the junctions between

domes, columns becoming inclined, and io

some extent pseudocolumnar, The domed bio-

strome pattern is repeated im the overlying un-

dulose and pseudocolumnar bed (D), again

passing up into long, parallel columns (E),

once more overlain by laterally linked and

pscudocolumnar lJayers (F), Gritty, cross-

bedded Jimestone overlies the stromutolitic

seyuenee.. Contacts between the various units

cannot be accurately placed in the field, clive

tO poor exposure and lJichen cover, but were

Hg W. Vo PREISS

pardy deduced from jaboratory study of speci-

mens (Fig. 8).

Column Shape and Arrangement: Unit (A)

consists at short, yertical to slightly inclined

columns, 5-20 mm wide branching frequently

from u wavy laminated layer. Columns swell

and constrict slightly, bear rounded bumps and

vecusional ribs, and coglesce frequently. Some

columns terminate their growth as pointed pro-

jections (Figs, 7), Kk. 1 978); overlying unit

(B) in part. columnar Tf present, columns

broad, up to 6 em wide, with very irregular,

bumpy outlines and numerous massive bridges.

grading laterally ond vertically into pseudo-

columns. with uvecusional interspaces, In the

main columnar units (C) and (E), columns

1-3 cm wide, swelling and constricting slightly

(Big, 17d. c). A few branches develop only

inta short, puinted projections (Fig. 7f, g).

Length of long, parallel columns between

Brunches 5-2(h.cm; the unit asa whole attuins

a thickness of up to 2m. but columns. not con-

linuous thrsughout, as pseudocolumnar hori-

zons intervene. ‘I famsverse

rounded polygonal, lobate. elonguted or irre-

gular: circular sections relatively rare, At dome:

edves, colunins slightly inclined (never at less

thun 607 to the horizontal), and bridged to

a greater extent, forming pseudocolumns

resembling those in units (B) and (D) (Fiz.

7d. im)

vi iat ow nf

Nadeau 1 L,

= eweneel BAA iat

jal PAVE YE 4 SY

‘ haces Fisas¥s ay rae

Soy es t+ Et

pb io!

Voncbir bide

Sy Deyatenent ef snes

Fig. § Disgrimmatic section of stromatolitic

bed near Kulpara. The felalive positions

of the specimens weie partly determined

in the field aml partly dednced from

laharntary specimens,

sections generally’

Branching: Basal columns of unit (A) chacac-

tenzed by frequent, slightly divergent branch-

ing (Fig 7}, k. 1). Long, parallel columns of

units (C) and (8) entirely a and A-parallel

branching, Near their biases, broad columns

and pseudocolumns (4-6 cm wide) hreneh

into several I—3 em columns. Above this level,

az and @-parallel branching moderately fre-

quent. Coalescing of neighbouring columns is

as frequent us branching.

Margin Siructire: All columus have a mark-

edly bumpy literal surface; bumps 0,5—1.0 cm

wide, with a relief of 1-5 mm most com-

mon, Most equidimensional, some grade into

short transverse ribs, others into short pointed

projections (He; W, 2), Longer pointed projec-

tions (up do 3 cm) moderately rare (Pig. 72)

Delicite bridges, compased of only one or twa

laminac very frequent, linking most adjacent

columos (Pig, 17d), usually depressed, U-

shaped (only the more prominent bridees

could be shown on reconstructions). Massive

bridges up to 2 ¢m thick moderately rare. Suc-

cessive delicate bridges in places only 5 mm

apart. Oecasionally very short peaks project

down from the column margins. Wherever

peaks and bridges do not occur. wall well deve-

loped. Wall most extensive in the lang, nurrow

columns. Laminae thin towards margin, and

coat suffuce for a distance of tip to | 5 em.

The wall involves from one to five laminae

(Fig. 17d, ©). ‘Vhe short basal columns of unit

(A) have only a patehy wall, as do some of

tke Jong columns with gently convex laminue

(Fig. 17b).

Lamina Shape very variable; generally narrow-

est columns have steepest laminae. while browd

basal columns and pseudocolumns have gently

convex and rectangular laminae. OF the

laminae measured, 695% have ratios of h/d

between 0.3 and 0.8, bul narrow columns and

projecnons usually have h/d greater than 1.0

(Fig. 10h). Fig. 9h illustrates coniinonty oeeur-

ting lamina shapes, Most laminac gently wavy.

usually with wavelength 2-3 mm.

Microsrruenire: Lamination indistinet «and

streaky (Eig, 17d, e), Where best preserved.

fairly continuous wavy dark liminae persist

from wall to wall, and alternate with light

tuminae. Dark laminae composed of very fine

grained silty limestone, consisting of equi-

dimensional xenatopic calcite of prain size

0.003-0.01 mm. with included subrounded

quarté and a little feldspar, ol grain size up

100.08 ran. Dark laminae 0.05—0.4 mim thick,

SOUTH AUSIRALIAN STROMATOLITES II

SA Depecttient oF Mines

. Examples of lamina shapes of the stramatolites, traced fram thin sections. (a)—Camephyton

garganicum garganicum: (b)—Gymnasolen cl. ramsuyi, (c)—lasgeria cf. tyonrest; (d)—in-

zeria conjuncta, (e)—Inzeriq: multiplex, (£)—Jurusania burrensix, (g)—Katavia cosratay (bh)

—Kulparia kulparensts.

generally thickest in central part of a column,

Boundaries’ diffuse. At column margins, dark

laminae thin to a thickness of about 0.05 mm

and coat surface of column. Intervening, light

laminue thinned more, and lens out some dis-

tance down the wall. so that here dark Jaminuc

merge. Light laminae up to 0,7 mm thick in

central parts of steeply convex laminated

columns. bul. thin rapidly towards the edges.

They consist of inequigranular xenotopic to

hypidiotopic calcite of grain size 0.015-0,05

mm, with minor rounded quartz. silt, of grain

size up to 0.08 mm. In the shert columns of

unit (A) lamination is better preserved (Fig.

{7f), Dark. homogeneous laminae, 0.15-1.0

mm thick, are composed of pale brownish and

greenish pigmented, almost equigrunuliar xeno-

topic calcite, of grain size 0,003-9.01 mm,

with inclusions of detrital quartz silt of grain

size 0.02-0.04 mm. Ih places, they have sharp

lower boundaries, but grade upwards into light

laminae, which are 0.3—1.5 mm thick, but thin

towards the column miurgins, and are com-

posed of slightly coarser, silty, xenotopic cal-

cite, of grain size 0.015-0.02 mm. Detrital

quartz grains are up to fine sand size (0.2

mm). All laminae extend uninterrupted across

the width of columns, unlike laminae in the

upper, long patallel cotumms.

Interspuces. wenerally very narrow {1-5 mm)

in units (C) and (EF), but wider in basal

columns of unit. (A). Their sedimentary’ fill

includes medium to coarse clastics, both terri-

genous und carbonate. Generally. quartz much

coarser than that incorporated inta columns,

The sediment consists. of approximately 40%

quartz (well-rounded, grain size 05-3 mm,

finer vrains tending to be subangular), 3%

feldspar {rounded to subangular cloudy micro-

NEI

MEAS RLD

Fig. 10, Frequency

SN, Deparemenc af Mires

distribution of lamina convexitics h/d for stromatolites iWlustrated in Fig. 9.

116

cline, up to 3mm gran size), 5% rack frag-

ments (rounded fragments. up to 4 mm, of

quartz-feldspar rock, quartvite and rare chert),

30% ¢arbonate allochems (inehiding fiat

pebbles 2-4 min Jong, flat pebbles coated with

3 or 4 pale and dark luminoe, recrystallized

oaids with dolomitic rims and rare composite

grains cemented by dark dolomitic rims) and

20% cement (sparry, hypidiotopic mosaic cul-

cle, of grain size O.015-0.06 mm cementing

allochems and lerrigenous detritus. in places

replacing the rims of these grains), Sediment

poorly bedded. Presence of wall between

bridges on columns indicates that sediment was

filled in periodically. Aller one influx of sedi-

ment, a bridge formed over it, then the inter=

space remained vacant while the column grew

another centimetre wor so. before the next

influx.

Secondary Alterwton; During diagenesis, the

carbonate of the long columns was partly re-

crystallized and dolomitized; some dark lami-

nue were preterentiglly dolomitized. and clays

were apparently redistributed inte a fine net

work of cracks and stylolites (Fig. (7e). In

places, the shape of laminae is completely dis-

rupted. Near the dome margins, lenticular

patches of spurry calcite occur within columns,

either concordant with the Juminae or at a

high angle to them. Vhese structures predate

clastic dykes which cut both stromatolile

columns and interspace sediment (both of

which must have been lithified at the time}

(Fig. 176). The filling af the dyke consists of

angular to subrounded, poorly sorted quartz, of

grain size 0.05-1 mm, The sand is tightly

WY:

PREISS

packed, the finest angular grains forming the

matrix. Calcite cement is almost totally absent}

quarl% grains are coated with iron oxide tims

In places, the filling process has actively eroded

the walls of dykes, so that disoriented trag-

ments of the surrounding Jimestone occur as

inclusions in the sand (Fig, (7b), Vhe dykes

probably formed by jointing of the alneady

lithified stromatolitic bed. especially between

adjacent domes, Concordunte stylolites, caneen-

trated at definite levels in the structures, Where

ihey are anly 1 or 2 mm apart, clearly post-

date the sand-dykes. Stylolites purtly follow

the tamination. and partly cut across i, Ver-

tical calcite veins up ta 1 cm wide, consisting

of course, euhedral crystals, post-date the stylo-

lites, and ate especially prominent in the junc-

lions between domes, which were persistently

subject t jointing. Dolomitization apparently

post-dates the formation of veins and stylolites,

und ts therefore yery late diugenctic.

Comparisons

These stromatolites have already been com-

pared to other groups. Ku/puria ktlparensis is

distinguished from K-. alieia (Cloud and Semi-

khatov) Walter, by its frequent delicate

hridges, generally more steeply convex laminae,

and by the presence of moderately frequent

pointed projections.

Distrihution; Etina Formation equivalent,

Umberatana Group, 7 km south of Kulpara,

northern Yorke Peninsula, ‘S$. Aust.

Age. Laie Adelaidean, correlated with the

Late Riphean or Vendian of the USSR-

Acknowledgements

T am indebted to Prof. M. + Glaessner for

supervising this study, to the support given

by the Centre for Precambrian Research, Uni-

versity of Adelaide, and to Dr, M, R, Walter

for discussions and collaboration, Drafting by

the Dralting Branch, Department of Mines,

und by my wife, i3 gratefully acknowledged,

This paper is published with the permission of

the Director of Mines.

REFERENCES

Brerrrano, J. (1968)—-Tes édifices stromatolt-

tigques préeambriens de la “Série & stranto-

tolircs” du Nord-Quest de IAhaggar (Su-

hara). Bil. Soc, geol.. Fr. 7( 10), £68-178-

BERTRAND-SaRFATI, J. (1972), Paléoécologie ve

certains stromatolites en récifs des formdtions

du Précambrien supérieur du yvroupe d'Atar

(Mauritanie, Sahara Occidental): création

d'esptces nouvelles, Pakwoveogr,, Palaco-

climatol.. Pataceecol. U1, 33-63.

Croup. PL E.. & Seminmatrov, M, A. (1969),

Proterozoic stromatolité zonution Am, J. Sei,

267, 1017-1061,

Gi arssner, M. F., Preiss, W, Vi, & WALTER.

M. ®. (1969). —Precambriaun columnar stro.

matolites in Australia: morphological and

Alfuligraphic analysis. Scierive 164, 1056-1058.

Komar, VY, A, (1966),—Stromatolity verktinedu-

hembriyskikh otlovhery severa stbirskoy

platformy | jkh stratigraticheskoe znachenie.

SOUTH. AUSTRALIAN STROMATOLITES IL 117

(Stromalolites of the upper Precambrian de-

posits of the North Siberian Platform and

(heir stratigraphic significance). Trudy geol.

Tayt. Leningr. 154, 1-122.

Komar, VY. A., Raaben, M. E., & SEMIKHATOV,

M. A. (1965).—Konofitony Rifeya SSSR i

ikh stratigraticheskoe znachenie. (Conophy-

tons of the Riphean of the USSR and their

stratigraphic significance). Trudy geol, Inst.

Leningr. 131, [-72.

Korovyuk, 1. K. (1963).—Stromatolity verkh-

nego dokembriya. (Stromatolites of the Upper

Precambrian.) /2 ‘“‘Stratigrafiyns SSSR” 2,

“Verkhniy Dokembriy”. (Moscow: Gosgcol-

tekhizdat.)

KryLov, 1. N. (1963)—Stolbchatye vetvya-

schchiesya stromatolity rifeyskikh otlozheniy

Yuzhnogo Urala} ikh znachenie dlya strati-

grafii verkhnegao dokembriya. (Columnar

branching stromatolites of the Riphean de-

pesits of the Southern Urals and their sig-

nificance for the stratigraphy of the Upper

Precambrian.) Trudy geol. Inst. Leningr. 69,

1-133.

Kryiov, I. N. (1967).—Rifeyskie i nizhnekem-

briyskie stromatolily Tyan’-Shanya 1 Karatau.

(Riphean and Lower Cambrian stromatolites

of Tien-Shan and Karatau.) Trudy geol. Inst.

Leningr. 171, 1-76.

MasLoy, V. P. (1937)—O rasprostranenii kar-

bonatnykh vodorosley v_ vostachnay Sibiri.

(On the distribution of calcareous algae in

Eastern Siberia.) Problemy Paléont. 2-3, 327-

342.

Preiss, W. V. (1972).—The systematics of South

Australian Precambrian and Cambrian

Stromatolites. Part I. Trans. R. Soc. 8. Aust.

96(2), 67-100,

RaaBen, M. E. (1964).—Stromatolily verkhnego

rifeya Polyudova Kryazha; ikh vertikalnoe

vaspredeleniec. (Stromatolites of the Upper

Riphean of the Polyudov Mountain and their

vertical distribution.) Byull. mosk. Obsheh.

Ispyt. Prir. Qtd. geal. 39 (vyp. 3), 86-109.

RAABEN, M. BG. (1969).—Stromatolity verkhnego

rifeya (Gimmnosolenidy). (Upper Riphean

stromatolites (Gymnosolenida).) Trudy. geol.

Inst. Leningr. 203, 1-100.

Rozanoy, A. Y., MIssarZHEVsKIy, V. V., VOL-

kova, N. A. Voronoya, L. G., KRYLOV,

I. N,, Ketter, B. M., Koro.yux, I. K.,

Lenpzion, K., MtkHWYyAK, R,, PyYKHOVA,

N. G., & Stporov, A. D. (1969) —Tommoat-

skiy yarus i problema nizhney granitsy kem-

briya. (Tommotian stage and the Cambrian

lower boundary problem.) Trady.. geol. [nst.,

Leningr. 206, 1-380.

SEMIKHATOV, M. A. (1962),—Rifey i nizhniy

Kembriy Yeniseyskogo Kryazha. (The

Riphean and Lower Cambrian of the Yenisei

Mountaing) Trudy. geol. Inst. Leningr; 68,

1-242,

Semikuatov, M. A., Komanr, V. A., & Sereprya-

Kov, 5. N. (1970)—Yudomskiy kampleks

stratolipicheskoy mestnosti. (The Yudomian

Complex. of the stratotypical area.) Akad.

Nauk. SSSR Trudy. 210, 1-207.

STEINMANN, G. (1911).—Uber Gymanosalen ram-

sayi, cine Coaelenterate von der Halbinsel

Kanin, Ball, Soc, geogr. Finland. 31, 18-23.

Wacter, M. R. (1972).—Stromatolites and the

biostratigraphy of the Australian Precambrian

and Cambrian, Palaeontology, Spec. Paper,

No. 11.

LIK

Fig. VI.

Fie. 72.

Fig. 15.

Fig, 14.

Fig, 15

Figy 16

Fig. 17,

W. V, PRETSS

Conophyton gargauea¢n gareqnicaum, from a vatt in the Paratoo Diapir: (a)—Near-axrul

section in outcrop of two adjacent columns illusirating murgin structure. The pen is 15 om

lung. Arraws indicate regular column margins; (b)—Transverse sections of ¢olimns in out-

trop. illustrating hoth circular and lanceolate shapes. The pen js 1S ¢m long; (c)—Qutcrop

section of broadly domed basal zoie, which gives rise upwards to conically laminated volumns.

(j—Thim section of crestal zone, brecciated perhaps hy compacuon of lithified Llaminne

Specimen No, S277; (¢)—Details of lamination. iustrating macrolaminae, detrital earbon-

ute granites (indicated by arrows), und swelling of some laminac. ‘Thin section. specimen

No. $214; (f}—Details of crestal zone illustrating contorted and thickened famination, Axial

lpnatludinal seclion. Thin section. specimen No, $932.

(al—Conaphyten yarganicum gargenicuny (Spec. No. $214). Longitudinal axial thin vectian

iMusirating erestal zone, laminstion, and deflexed margins of kiminge. The thick continues

bands are actually otacroalaminae. Natural ssizeé; (b), (c)—Gynmasolen of. ramsayi, From

boulders in a conglomerate in the ‘Vapley Hill Formation, near Wilson. Flinders Ranges:

(b)—-S388. Longitudinal thin section of verticul, branching cclumns, with iniraelust breccia

in iuterspaces, Natural size; (¢)—S387, Longitudinal thin section of joclined columns inter-

preted us derived from a bioherm murgin.

(uI—Gyenoselen cf. ramsevi from near Wilson. Longitudinal slab of regular walled

columns interpreted to be derived from a bioherm centre. Specimen No, S388; (b) to (¢)—

fuzevia ef. tomtsi, from the middle limestane of the Wundowie Limestone Member, Burr

Well, northern Flinders Ranges: (b)—Colomnar purtiun of a hioherm illustrating columns

with niche-projections. Note siylolites at base: (¢)—Domed basal part of bioherm with

continuous lamination; the upper columnar portion is separated by a stylolitic zone, Hammer

is 3 em Jong, (d)—Columnar zone overlying continuausly laminated basal purtion of bio-

herm. Note stylolitic zone ut pencil point. Pencil 17 cm long: (e)—Longitudinul thin section,

illustrating subeylindrical columns with altered margins and interspaces, gently convex to law

Makes anaes and a niche-projection, ‘Ehe basal part is iuensely cut by stylolites, Specimen

Oo, S452,

(a), (b)—Hizeria conjuncta, Brighton Limestone equivalent, Depot Creek, southern Flinders

Runes} (a)—Longitudingl thin scetlon of broad, basal coldains with niche-projection, The

laminae are allernaling dark, dolomitic, and light, calcitic, Holotype, $442; (b)—Longitudinul

thin section of inclined, tubcrous columns from bioherns margin. Specimen No. S4uds ic),

(chi—Jnzeria multiples, Brighton Limestone equivalent. west of Mount Remarkable, southern

Flinders Runges; (c¢)—Longiludinal thin seution of vertical columos, Natural size. Molotype,

S385; (d)—Longinidinal slab of same 4pecimen.

(2)—Inzeria mittipler, Brighton Limestany equivalent, east of VYednalue, southern Flinders

Ringes. Longitudinal thin seclion. Specimen No, 849; (b) to (e)—Jurusania brirrerists,

upper limestone of the Wundewie Limestone Member, Borer Well, ourthern tlinders

Kunges: (bJ)—Smooth eylindrical vertical columns near a bioherm margin. Hammer is 30 en

longa: (c)—Contiguous Spherieal bioherms; ()—T ongitudinal thin scetion iMustrating di-

chotomois s-parallel branebing bi cylindrical columns, Specimen No. S482: (e)—Lon-

gitudinal thin section of narrower cylindrical columns with slresky microstrocuire: Holotype

$543.

(a) Jernsdeiq barvensix. Longitudinal thin seetion of columns anising from undulating

slromatolites at buse. Specimen No, S481; (Bb) to (d)—Karavia cosata, from colomitic

‘inember" of the Brighton Limestone, Depot Creek: (b)—Long, vertical columns in longi

tidinal wulerop section. Hammer is 30 em lung. (¢J]—Transverse section of columns in out.

crop, Pon js 15 ¢m long; (d)—Longitudinal thin section iNustrating indistinet hirunation

and walled columns. Interspaces are lilled with sandy dolomite. Holotype, S!75. Natural

size. (¢)—Ardparia kalparensis, Etinn Formation equivalent, Kulpara. Parr of outcrop of

ovlindrical columns. Pen is 15 em Jong.

(u)}—Katavia costata, Brighton Limestone, Depot Creek, southern Flinders Ranges, Margin

of a bioherm showing inclinalion of columns ut right of photograph; (b) to (fF) Aulparia

ladparensis, Btina Formation equivalent, Kulpari. northern Yorke Peninsula; (b)—L.ongi-

tudinal thin section illustrating a sand dyke post-dating the lithification of the stromatolites.

Incorporated tn the dyke filling are fragments of the wall rock. Specimen No, 5420: (ce s—

Ouitrop transverse sections of lobute columns. Pen is 15 cm long, (d), (¢)—Longitudinal

(hin scetions of columns; holojype S380; (f)—Smoall irregular columns from Unit A at the

lose of the bed: longitudinal thin section. Specimen No. $270.

SOUTH AUSTRALIAN STROMATOLITES II

FIG,

PREISS

W. V.

120

FIG,

SOUTH AUSTRALIAN STROMATOLITES II

FIG.

SOUTH AUSTRALIAN STROMATOLITES II

W. V. PREISS

FIG.

SOUTH AUSTRALIAN STROMATOLITES II 125

STUDIES ON SOME SPECIES OF HAKEA (PROTEACEAE)

BY J. R. MACONOCHIE*

Summary

MACONOCHIE, J. R. (1973).-Studies on some species of Hakea (Proteaceae). Trans. R. Soc.

S. Aust. 97(2), 127-133, 31 May, 1973.

Hakea standleyensis sp. nov. is described from Standley Chasm, central Australia. This species is

allied to H. collina C. White of south-west Queensland but differs in leaf size and flexibility, and

fruit shape.

An examination of collections under H. multilineata has led to the recognition of five species:

H. multilineata Meisn., H. francisiana F. Muell. and H. grammatophylla (F. Muell.) F. Muell., and

two new species, H. minyma Maconochie and H. coriacea Maconochie. H. bucculenta Gardn.

which is allied to this group, is readily separated by its narrower uninerved leaves. The possible

evolutionary origins of the species in the group are discussed in relation to their distribution.

STUDIES ON SOME SPECIES OF //4KEA (PROTEACEAE)

by J. R. MaAconocie*

Summary

Maconocult, J. R. (1973).—Studics on some species of Makea (Proteaceae). Drans. RK. Sac,

S. duye 9702), 127-133, 31 May, 1973.

Hakew standleyensiy sp. nov, is deseribed from Standley Chasm, central Australia, This

species is allied to

flexibility, and fruit shape.

An examination of colleetions under H,

H. callinad ©. White of south-west Queensland but differs in leaf size and

muutilineata has led to the recognition of tive

species: A, multilineata Meisn., Hy franecisiana FP. Mucll and 2. grammatophylla OP. Muell.)

Fk. Muell., and lwo new species, HM. minveui Maconochie and M7. cariacea Mivonochie. Jf.

bueculenia Gardo., Which is allied to this group, is readily separated by its narrower uni-

nerved leaves. The possible evolutionary ovigins of the species in the group are discussed in

relation to their distribution.

1, Hakea standleyensis Maconochie sp. noy.

Frutex erectus diffusus, usque ad tom altus. Folia

linearia, teretin, erecta, infirme pungentia, circa

L5 mm diam. 30-65 mm longa (sed usitite

50-60 mm). Inflorescentia axillaris, racemosa,

parva, 6—-9-flora, rachide cu, 2 mm longa. Flores

ca. Bel] mm longi, per pilos longas sericeas albos

villosa, perianthio 4-6 mm longo atque pedicello

4-5 mm loneo. Ovarivm glabrum puene sessile,

ca, | mm longum, stylos glaber, ruber, ca. 9 mm

longus; stigma late conicum, ghabrum. Turns

obliquus, ghins rubra, semiannularis ad elongatum,

ca. | mm longa. Frveras ca. 15 mm longus, late

fulcalus, ca. 5 mm Intus Cad partem latissimam ),

pericurpo verruculoso, pedunculo ca. 10 mm

longo. Seminis corpus obovatum, ad apieem atten-

uatuim, cau. S mm longuni: ala ca, 5 mm longa,

reticulo tenui brunneo praedita,

Holorypus: D. J, Nelyon 1556, Standley

Chasm (23°41/S. 133°27'E). 53 km W of

Alice Springs, N.T. 19.ix.1967 (NT).

Iyvoiypis AD, BRI, NSW.

Specimens examined (all from Standley

Chasm). Chippendale & Johnsen (NT

3997), 16.x.1957 (AD, BRI, CANB. K.

MEL, NSW. NT, PERTH); Muconachie

464, 25.vili.[967 (NT); Nelyon 1555,

1Qin.1967 (MEL. NT): Must 356,

OX.AL9IOS (NT),

Erect straggling shrub up to Lom high.

Leavey linear. terete. weakly pungent-pointed,

erect on stems, about 1.5 mim in diam, and (30—)

50-60 (-65) mm long. Jnflorescence a srnall

axillary raceme of 6-9 flowers, the rachis

about 2 om long, villous with long white silky

hairs, Flowers about 8—LI mm long. perianth

4-5 mm long, pedicel 4S min long. Ovary

glabrous, almost sessile, about 1 mim long; style

glabrous, red, about 9 mm long; stigma

broadly conical, glabrous. Torus oblique:

gland red, semi-wnnular to clongate, about 1

mm long. Fra about 15 mm long, broadly

sickle-shaped, ubout 5 mm broad at the widest

point; pericarp verruculose, peduncle about

10 mm long. Seed-body obovate, tapering to

apex: about 5 mm Jong; wing about 5 mm

long with fine brown reticulations.

Habitat: on and in quartzitic rock ledges and

crevices almost at summit of maih outerop

ut reur of Standley Chasm.

This species is endemic to the Miedonnell

Ranges, central Australia, being found only

at high altitudes at Standley Chasm. Chippeo-

dale (1963) discussed the relic nature of plants

found in the Macdonnell Ranges und ft is pro-

buble that H. standlevensiy is a relic species,

possibly on the verge of extinction,

Hl. standlevensis is allied to H. colling C,

White (1944, p, 79) and also A. iiicracarpe

R, Br. H. collina is found on the sandstone

tableland of south-west Queensland and 7,

micrecaurpa is restricted to southern) highland

areas of castern Australia and extends down

to Tasmania. The three species may be separ-

ated as follows:

= Aril Zone Research Institute, N/T. Administration, Alice Springs, N.T. 5750.

128 J. R. MACONOCHIE

(1) Perianth glabrous. Leaves terete or trique-

quetrous a, coe. Hy microcarpa

(1) Perianth villous. Leaves terete.

(2) Leaves flexible, (30—)50-60(-65)mm

long, weakly pungent-pointed. Follicle

about 15 mm long, 4-5 mm wide, in-

curved along ventral edge . ;

FH, standleyensis

(2) Leaves rigid, 20-40 mm long, strongly

pungent-pointed, Follicle about 20 mm

long, 6-8 mm wide, almost straight

2 H. collina

along the ventral edge .

WERDARIUM. OF NE

ALICE GPRM

Fig. 1.

Il. Hakea multilineata and its allies

Bentham (1870) commented that he could

see no major difference between the descrip-

tions of H. multilineata Meisn. and H. gram-

matophylla (F, Muell.) F. Muell., except that

the raceme of the latter species has a densely

tomentose rachis, Bentham therefore con-

sidered H. grammatophylla as a variety of H.

multilineata, Black (1948) followed Bentham.

Bentham also placed H. francisiana F. Muell.

under H. multilineata although he did not see

HOLOTYPE

HEABARIUM OF MOATHERN TERRITORY

Eqvings, Auewabs

fe NT, ug

: ‘,

Ne Tae bien StS ye

(tip ae La, fee :

' Call Det

‘ Nates » ns ‘

Se pe

Holotype sheet of Hakea standleyensis Maconochie.

STUDIES ON SOME SPECIES OF HAKEA (PROTEACEAE)

any material of the first species. Eichler (1965)

treated A. francisiana as a separate species,

To study this problem further, collections of

this group of species were borrowed from the

principal Australian herbaria and also two type

sheels fram Kew and New York Botanic Gur-

dens, Data were compiled on inflorescence

length, colour and texture, the shape ond size

of fruit and seed, and lIcaf dimensions and

number of veins. The collections were initially

sub-divided into six groups based on gross simi-

larities and dissimilurities and then the mean

and standard deviation of the numbet of veins

per leaf (6 to 12 leaves per sheet) for each

group culculated, A t-test was then applied to

the data.

H. multilineatfa and its allied species have

the following similarities: all are shrubs; leaves

linear, flat with several to many nerves; infie-

rescence a many flowered raceme 2-I() cm

long, enclosed in bracts at the bud stage: stig-

matic cone long and narrow; fruit almost ses-

sile.

In general, the flowers of H. coriueeu, H,

francisiana, H. grammatophylla and H. multi

lineata are very similar. H. ntinyma differs by

having much smaller creamy-white flowers

(pink to red in the other specics),

H. hucculenta Gardn. (1936, p. 123) is

allied to this group of species in that it has a

raceme of similar size, shape and colour, simvi-

lar fruit. but differs in that its leaves are much

narrower und uni-nerved,

The mean number of veins per leaf, the

standard deviation and sample size are pre-

sented below—

Mean St, Dev. Sample size

A. frencisiana 6.0 1.3 182

H. grammatophyvila 7-1 1.4 84

H_ curtacea 10.3 5 163

ft. minyma 142 2.0 a9

AL omuledlineata 15.1 3.4 156

The probabilitics and t-values for difference

of means between species are presented in

Table 1.

TABLE 3}

Species 1

| A. cériaced 28.4 15.6 16.8 TWA

2 OH, francisiana ea 3.9 38.0 35.5

3H. grammataphylia <001 <,001- 27.0 21.6 tvalues

4 H.minyma <.001 << .001 << 001 25

5, ntultilineata <<ool <<00l <<001 .O1<P<.02

Probabilities

on ———————————

Thus at the 5% probability level, the sample

means of all species significantly differ from

each other. When the number of veins per leaf

is used in combination with inflorescence

length and size, pubescence on rhachis, und

fruit shape, then these species cai be readily

separated,

Key 10 Hakea multilineata aad allies

| Leaves with one distinct central vein

i, bucerlgata

1, Leaves with several to many veins -— — - 2

2, Muatuce fruit with distinet bicarinate ventral

suture Ssnbie d) H. niultilineqia

2. Mature fr wit “without bicarinate ventral

suture. vith fo bie eseterorsaryel np

3. Perianth creamy white _H. minyma

3. Perianth pink ta red. _... satlecsleeapitltrdte EE

4. Rhachis of infloreseence ‘tamentosc a.

HT. prammatophylta

4, Rhachis of inflorescence glabrous .___ 5

5. Main veins of leaves 5 or 7 (-8). Leaves 3-6

mm wide ....., ... A, francisiana

§. Main veins (8) 9-10. (- 13). Leaves 6-16 mm

wide ...... A. eoriacea

Hakea bucculernita Gardner 1936: 123.

Holotype: Gardner 2571 (PERTH) (n.v.)

Distributian: Restricted to Western Australia

from Galena in the north to Geraldton in the

south (Fig. 4).

Selected Specimens: W. Aust., Blackall 4709,

48 km N of Galena, 18.ix.1951 (PERTH);

Ginins 1550, 51 km S of Wartoo road house,

north of Geraldton, Aug. 1967 (PERTH):

Long 25, 129 km E of Geraldton, I.vii- 1960

(PERTH).

Hakea multilineata Meisn. 1847: 261,

Holotype; Drummond coll, fll no. 275, Swan

River (NY).

Tsotvpes: K (twa sheets);

MEL 1010216; PERTH.

Distribution: Restricted to an area in

MEL 10102132,

the

bau

south-west cotner of Western Australia (Fig,

5),

Selected Sperimens; W. Aust., Brooker 1872,

66 km EB of Brookton, 22.vii. 1969 (PERTH);

Drummond 275, Swan River (Vype) (K,

MEL, NY, PERTH); Filsen 8903. Holland's

Track, 88 km SW of Coolgartlie, 14.19. 196h

(MEL{, Wily 3220. ca, 120 km W of

Diniell on road wo Lake King, 15ix. 1964

(AD),

Hakea prammatophylla (F. Muell,) F. Mucll.

léh7- Zi.

Bayionyin, Grevillea grammatopliyla P. Muell.

1865; 24.

Holutype: “tn Australia centrali prope ecatral

Mount Stuart fructicibus intecspersa”, J. Wred.

Staart (MBL 1010236),

Mueller (1867) cited RK, T. Sullivan—-

“Guwler Ranges” and M, Weidenbach, “in

vicinity of Port Lincoln”, as 72, graumrate-

pivile but these two specimens are A. fronci-

siava FP. Muetl. The tragmentary nature of the

specimens probably explains the misidentifica-

tion.

Distribution, Restricted to the

central Australia (N.T.) (Fig. 5).

Selected Specimens: NLT. Beauglehole 23189,

King’s Canyon, George Gill Range. Svil. 1967

(NT, NSW)> Lothian 76, Standley Chasm,

Juty-Aug. 1954 (AD); Macorechie 443, Ser

pentire Gorge, 19.vil, 1967 (NT),

Makew minyma Macoiiochic, sp, nov,

Feutex L-2 m altus, caulibus mojoribos nonnullis

Peaeditus. Folia erecta, linearia, elongata, plana,

fuevia, glabra, rigide corincea, 8-15 em longa, 5-8

mm tata, o [4-17 nervis. (usitale 15) lineata, si-

floreseentia racemosu multiflora, thuchide glabra,

4-5 om fonga. Flores. maturi et expansi 8-9 mm

Jong. Perianthinm gilvam, glabrum: torus circa

| mm langim, OS ma tatum, horizontatls vel

aliquantum obliquus, Ovarium pane sessile, gluh-

ram, 1-15 nim longum; stylus glaber, filiformus,

3-6 mm longus; stigma labrum, ercetum, coni-

cum, 1 mo longum, Glans ovoidee—globosa, ad

basin avarii sita, Frets ovoideo—globusus, 2—

25 eny Jongus, 1-1.5 cm Jatuy: pedicellus 1-3 mm

longus vel minusculus; rostrum perconspicuum,

saepe curvatuin, Pericarpus laevis nisi pustilac

Parvae, plus minus straminicolor. Semiuls serpus

8 mm longum; ala 1.? em Jonga, nigra. rhombi-

formis vel angilato-ovata, secus corpus imilatera-

liter, decurrens-

Holotvpus: Macanochie 846, about 84 km

W of Musgrave Park Station, S. Aust. (26°

20'S; 130°30’B), 30.ix. 1969 (NT). Speci-

men with flowers, fruits and photograph.

iwaiypie AD, BRI, CANB, K, MEL, NSW

MERTH,

ranges of

J. R. MACONOCHIE.

HM. microneura C. A. Gardner= nomen. inva-

lidum in Fairall (1970),

Strub (—2 im tall, with several main ytems-

Leaves crect, flat, tinear, elongate, smooth,

glabrous, rigidly coriaceous, 8-15 em long,

5-8 mm wide, with [4-17 nerves (mostly 15),

Inflorescence a raceme with numerous flowers,

rhachis glabroos 3.0-5.0 em long. Open mature

flowers 8-9 mm long. Perianth creuamy-yellow,

glabrous, torus about | mm long, 0.5 mm

broad, horizontal ta slightly oblique. Ovary al-

most sessile, glabrous, 1-1.5 mim long: style

glabrous, filitorm, 5-6 mm long; stigma pliab-

rous, erect, conical, | mm long. Gland ovoid-

globular, at base of ovary. Fruit ovoid-globu-

lar, 2-25 em long. 1-1.5 cm broad; pedicel

[—3 mn or Jess; beak strongly developed, often

curved, Wall smooth with small pustules, col-

oured beige to light tan, the Iutler colour often

more pronounced on beak. The beak is often

lost From fruit older than twelve months and

the wall becomes grey in colour, Fruit thea

1.9-2.0 em Jong and |.4-1.6 em brood. Seed

bedy & mm long; wing 1,7 cm long. black,

rhombic or angulato-ovate in shape, cecurrent

along one side of the body.

The specific epithet ts derived from the Pil-

jantjatjara word minyma (woman). an allusion

to the fruit's resemblance lo a woman’s breast.

Aistribution; This species extends from. ihe

Musgrave-Mann-Petermann Range complex

of South Australia and the Northern Terri-

tory down to the Tammin-Merredin urea in

the south-west of Westeta Australia (Fig, 5).

Seleered Specimens: ST. Duntop 2010, 48 km

NE of Mt, Davics Camp, Mann Runge, 31x.

1970 (AD. CANB, NT); Larz 941, ca. 129 km

NE of Mt. Davies Camp, edge of Pottoyi

Hills, N.T_, 2,xi. 1970 (DNA, MEL, NT), S

Aust, Eichler 17285, between Mi, Harriet and

Musgrave Park Homestead. S.ix. 1963 (AID):

Macererkie 846, ca, 84 kin W of Musgrave

Park Station, 30,ix, 1969 (Type) «NTI, W.

Aust. Gardner 839, Coolgardie, 4.x. 1920

(PERTH); George 2879. 35 km NE of Luver-

ton. 23.viil, L961 (PERTH); Gearge 5639, 55

km SW of Wiluna, 29%.vii, 1963 (PERTH):

Koch 975, Cowcowing, Sept 1904 (MBL,

NSW, PERTH): Rovee 4461, Comet Yale,

23.ix. 1953 (PERTH).

Makes francisiana F. Muell, 1858; 20,

Type: G. Francis, near bay, Spencer's Gulf.

Specimen probably lost (search made at AD,

K, MEL).

Nearype: RB. Copley 2345, Thirlga Station,

Cluwler Ringes, S, Aust, |3.x, 1968 TAD),

STUDIES ON SOME SPECIES OF HAKEA (PROTEACEAE) 131

i re

Shy emadeg-

ABOLIMHSL NYIHIHON 40 Wh”

fee

cae, FeO

WALOIOW

O yn

ivis

Woeveeay

Fig. 2 (above). Holotype sheet of Hakea minyma Maconochie.

Fig. 3 (below). Holotype sheet of Hakea coriacea Maconochie.

{72 ]

tl. anultilinedta vir gramined

lidum in Bairall (1970),

Disiribution: Widely distributed theougl the

southern arid areas of South and Western Ausa-

tralia (Pig. 4),

Selected Specimeny: S. Ausl Cornwall 56, ca.

SS km SE of Kimba. ivi. 1968 (AD. NV):

Rimyay $.n,. 113 km SSW of Camp 17. Elder

nomen iWyVva-

Expedition, July 1891 (AD, NSW): Wilyon

(573, 40 kor NW of Ceduna. las. 1960

(AD). W. Aust) Gardner 6465, Bencubhin,

T0.ix. 1942 (PERTH): Georve S646, 122 kin

™ of Sandstone, 29.vil, 1963 (NSW, PERTH):

Hilyvan 31442 ca. 30 km SE of Londonderry.

Idix. 1964 (AD, PERTH)

Distribution of A. fhuceutenta (m), H

coriuced (&), and Jf: franeisinne (®),

bin. 4.

RSs

hig 5.) Distribution of //. granunatophylla (®),

Ho ominyma (@). He miutrilineata (a).

From Kangaroo L, South Australia, there

huve been two sterile collections made of a

species close to /7. franeisiana, bur until better

material is availuble, its status is obscure,

Hakea coriacea Maconochie sp, nov.

Frifex 3-4 1 altus, Folia linearia elongata, plana.

eoriace’s intervenium pobescenti, 920 em Tonga.

usitiite [4-17 em. 6-16 mm lata usitate 8-10 mm,

» RK, MACONOUCHIE

s—l4 hervis interns plerumque 9 vel LOL Lafleres-

centia racemosa multiflora rose vel earneéa, cha.

chide glibra, @=! 1 em longa. Ploy glaber 23-25 mim

longus, pedicelluy 2-3) mm longus, perianthium

7-8 mm, stylus ghaber |9% 27 mm Jongus. stigma

Wabraum. conicum 1.5 mm longum. Torys ali-

qhanium cobliquus, ghins semi-annularis. Brae tea

elabra vel pubertila, caduea, marine ciliata.

Fractis ovoidea-globasus, circiler |& mnt jongus,

12 inm Jatus ef evassus, pericarpiis laevis nisi pus-

lulne putteae purvae vel aliquando fissuris paucts.

Affinis Haekede franeistinae Fo Muell sed differt

numero majoro nervorum et foliibus latrioribus.

Shrub to 3 to 4 m high. /eavey linear, Mat.

coriaceous, with a fine pubescence on the inter-

veinal area, 9-22 em long mostly 14-17 em.

6-16 mm wide. mostly 8-10 mm with S13

nerves. Inflorescence pink-red, rhachis glabrous

6-11 cm long, a raceme of many flowers.

Flower glabrous 23-25 mm long, pedicel 2-3

mm long, perianth 7-8 mm, style ghibrous

19-21 nin, stigmatic cone 1.5 mm long Terns

slighily oblique. ghind) semi-annular. Bracts

glabrous or sometimes puberulous with ciliate

margin, cuducous. Fruit woody. shortly pedun-

culite (2-3 mm) about 1S mm tong, 12 mm

wide and broad. wall smooth with w few small

pustules or sometimes with small fissures.

Closely related to AM. franciniane but differs in

greater number of nerves and wider leaves.

Holowpus: C. A. Gardier (2155, hetween

Perenjori und Jibberding, W. Aust. Sept.

1953 (PERTH).

Dis:ribmiien: Restricted to awn

WSW of W. Aust. (Pin, 4)-

Seleeied Speciinens: W. Aust. Aplin 1983.

3 kn EF of Tummin, 13.7%. 1962 (PERTH):

Drupiniond (8. W. Aust. (MEL. NSW);

Koch 1018. Coweowing, Sept, 1904 (AD,

MEL, NSW); Melville 4265, U8 km W of

Dalwaliina, 2l.vii 1953 (AD. BRI K.

MEL. PERTH).

ures in the

Phylogeny and Evolution

Tirese species form a natural group dillerine

from the other members of Benthan’s Hekee

scet. Conogvinoides ser. Longivivlee by the dis

distinctly elongate raceme, 2-10 em Jong. ‘The

other members of this series all have a more

compact raceme, resulting in a more globular

inflorescence.

The phylogenctic relationships of this group

are uneertain:

(1) The inflorescence. leaf and fruit structure

of HA. francisiena, HL. coriacea, MH. grammar.

phyvlla and I. bucealenra indicate they pro-

bubly have a common ancestor, and that J/

muiilineata and HH. tonvine may have evolved

independently,

STUDIES ON SOME SPECIES OF HAKEA (PROTEBACEAE) 133

(2) The similar distribution patterns of H.

frencixiane and H. minyma suggest that these

two. species may have had a common ancestor,

and //, coriacea, H. grammatophylla, H. buc-

culenta and possibly H. multilineata were all

derived trom Al. francivsiana.

The south-west province of Western Austra-

lia appears to be the focus of origin of this

group of species, as five of the six species

occur there and the distribution tends to

radiate from there into the more arid areas to

the north and cast.

The two records of Makeu ef. franecisiana for

Kangaroo Island suggest thal, during an ¢arher

geological period, Kangaroo Islund acted as a

migration bridge between Eyre and Yorke Pen-

insulas and Fleurieu Peninsula. Wood (1930)

refers to this connection and rewards it as

tecent in geological time.

The implication of these observations is that

either (1) this group of species may have

evolyed, diversified and migrated during the

period of a land connection between the Eyre

and Fleurieu Peninsulas or, (2) this was a

period of rapid spread of H. /ranersiana,

The restricted distribution of H. gramsiio-

phylla to the tanges of central Australia and

the distributional pattern of A. francisiana

would Indicate a north-eastern migration route

from the south-west province of Western Aus-

tralia, Subsequent periods of aridity would per-

mit speciation to occur as there was a retreat

to more favourable habitats.

Acknowledgements

The Directors and Curators of the follow-

ing Australian Herbaria (AD, ADW, BRI.

CANB, CBG, MEL, NSW, PERTH) are

thanked for allowing examination of their col-

lections and also Kew and the New York Bo-

lanic Gardens. for making available Drum-

mond’s type sheets,

To Mr. J, H, Willis, | am indebted for two

of the Latin deseriptions and to Dr. Hj, Eichler

for his advice on nomenclatural problems and

comments on the manuscript.

References

Benruam, G. (1870).—"Flora Australiensis™, Vel.

§. (Reéve: London.)

Brack, J, M. (1948).—Flora of South Australia’,

Part Il, 2nd edn. (Govt. Printer: Adelaide.)

CuHrpPpeNpALe, G. M. (1963).—The relic naire

of some central Australian plants, Trai, R.

Soe. 8. Asst. 86, 31-34.

Eicutrr, Hj. (1965).—*Supplement to J. M.

Black's Flora of South Australia”. (Govt.

Printer: Adelaide.)

Faimate, A. R. (1970).—“Western Australian

Nutive Plants in Cultivation’. (Pergamon:

Australia, )

Garpnern, C, A. (1936).—Contribuliones Florae

Australise Occidentalis No. IX, J. R. Soc. W.

Aust, 22, 123-128.

Meisner, C, F, (1848).—Jn ©, Lehmann,

“Plantae Preissianae” IJ, 260-262, (Hamburg.)

MUELLER, F. (1858) —“Fragmenta phytozraphisde

Australiae” Vol. LL (Govt. Printer: Mel+

bourne.)

MUELLER, F. (1865).—"“Fragmenta phytographiac

Australiae” Yol. Y. (Goyt, Printer: Mel-

bourne.)

MueELLeR, F, (1867)-—“Fragmenta phytographiae

Australiae” Vol. Vi. (Govt. Printer: Mel-

hourne.)

Wire, C. T. (1944).—Contributions fo the

Queenlsand Flora, No. 8. Proe. R, Soe. Qld

§5 (5), 79-80.

Woop, J. G. (1930),—An Analysis of the Vege-

tation of Kangaroo Island and the adjacent

Peninaulus. Trams. R. Soc. §. Aust, 54, 105-

139.

PHOSPHORIAN LAVENDULAN FROM DOME ROCK MINE,

SOUTH AUSTRALIA

BY A. W. KLEEMAN* AND A. R. MILNEST

Summary

KLEEMAN, A. W., & MILNES, A. R. (1973).- Phosphorian lavendulan from Dome Rock Mine,

South Australia. Trans. R. Soc. S. Aust. 97(2), 135-137, 31 May, 1973.

A new variety of the rare mineral lavendulan (= freirinite) has been found in Precambrian rocks in

South Australia. It is notable for containing a significant amount of phosphorous replacing arsenic.

Its formula, based on microprobe analysis, is (Naj.o7Ca1.91Cu4.go) (AS3.16P.s4)O16Cli ss 4H20. Powder

diffraction data are also recorded.

PHOSPHORIAN LAVENDULAN FROM DOME ROCK MINF,

SOUTH AUSTRALIA

by A. W. Kieeman* and A. R. MILNES}

Summary

KreeMan, A. W., & Micyes, A. R. (1973),.—Phosphorian lavendulan fram Dome Rock Mine,

South Australia. J'rans. KR. Soc, §. Ausf. 9742), 135-137, 31 May, 1973.

A new variety of the rare mineral lavendulan (= freirinite) has been found in Precam-

brian rocks in South Australia, It 1s notable for containing a significant amount of phos-

phorous replacing arsenic. Its formula, based on microprobe analysis, is (Nay .o7Car.o1Cuy.so)

CASy 43P.94)0i6Ch a5-4HeO. Powder diffraction data are also recorded,

Tntroduction

The Dome Rock mine is situated about 44

km ENE of Olary (148°27’R, 31°55/S). The

detailed geology of the mine area is described

by Dickinson (1942) and a brief description

is given by Campana & King (1958). The

country rocks are low grade metamorphics of

the Willyama Complex: Dickinson considers

the lodes ta be replacements of a fine grained

sandstone. The primary ore is reported by

Campana & King to be chalcopyrite and pyrite.

Some cobalt is found in the sulphides and ery-

thrite stuininys were reported by Mawson in

an unpublished report to the Dome Rock Cop-

per Mining Co, The fodes are oxidised to a

depth of about 60 metres. The oxidised ore was

inainly chalcocite, tenorite and cuprite, with

olivenite and chrysocolla.

Bayliss er al. (1966) examined specimens

of oxidised ore from Dome Rock and reported

several arsenic minerals occurring as “encrus-

tations alony partings in siliceous ironstone”.

They identified clinoclasite, Cu, AsO,(OH)..

conichalcite, CaCu(AsO,)(QH), and a third

mineral which they called chlorotile,

Cuy (AsO,)4.6H.O with the comment that it

also. =oresembled = mixite, Cu,,Bi(AsO,),;

(OH),,, 6H:sO. However, chemical tests

failed to reveul the presence of bismuth. They

also record the identification of cornwallite.

Cu, (AsO, ).(OH),.H,0 but do not quote

the authority, Their own identifications were

based on X-ray diffraction amplified by the

chemical test on the “chlorotile”.

Early in 1972, Mr, H_. Gallasch submitted

a sample from the 120 ft. level of Dome Rock

mine, containing a mineral which proved to

be quite different from any reported by Bay-

liss et al, The deseription of this mineral re-

sembles that of clinoclasite given by Buyliss

et al., but the powder patterns are dissimilar.

Tt occurs as rosettes of ucicular blue crystals on

u block of siliceous ironstone, The rosettes are

about 2-4 mm in diameter and the individual

crystallites are Jess than 0.02 mm_ across.

Broadening of the lines in X-ray powder phato-

graphs indicates that the mineral is in fact cx-

tremely fine grained. The powder X-ray photo-

graph suggested that it could be sampleite or

lavendulan (Guillemin 1956). Accordingly it

was decided to analyse it on the microprobe

ta confirm its identity.

Methods

A polished thin section of some fragments

af the mineral was examined in the C.S.1-R.0O.

Division of Soils’ “Geoscan” (Cambridge In-

struments) electron probe microanalyser, The

elements As, Cu, Co, Ca, Cl, P. Mg and Na

were detected during reconnaissance spectro-

meter scans, Chemical homogeneity of the

mineral fragments was checked by photo-

graphing X-ray scanning images of the ele-

ments of interest. Selected areas of the mineral

* Department of Geology and Mineralogy. University of Adelaide. Adelaide, 5. Aust. S001.

7+C,S.1.8.0, Division of Soils, Glen Osmond, S, Aust. 5064,

130

fragments were then analysed quantitatively

for these elements.

Under normal conditions of analysis!, stg-

nificant systematic drifts in count rate with

time were observed for all elementy. This effect

is possibly due to a combination of photo-

chemical degradation (McConnell 1969) and

thermal decomposition of the mineral under

the influence of the electron beam in the eva-

cuated specimen chamber (Sweatman & Long

1969). Loss of alkali elements from silicate

minerals with time under the influence of elec-

tron bombardment during microprobe analysis

is a well known but not fully understood

phenomenon (McConnell 1969; Siivola 1969),

and can be minimised by reducing the beam

current. In the present instance, however, the

count rate drift was. minimised by expanding

the electron bear so that it sampled a circular

area 50 microns in diameter at the specimen

TABLE i

Micruprobe analysis

1 2

AssO;, 36.4 44,8

cud 38,2 36.3

CoO 0.03 nil

CaQ 5.7 5.8

Cl 5.5 3,5

PO; 6.0 n.d,

MezO 0.04 od.

NasO 33 3.1

Total 95.2

O=Cl 1.2

Total 94.0

1. Lavendulan, Dome Rock Mine (analyst A. R.

Milnes)

2. Lavendulan, San Juan, Chile (Guillemin 1956)

TABLE 2

Stractural Formula Based an As-+ P—4

Na 1.070

Ca 1.014

Mg 0.010

Cu 4.800

Co 0.004

Total 6.898

AS 3.161

im 0.839

‘otal 4.000

of 1.553

A. W. KLEEMAN and A, R. MILNES

surface, and by driving the specimen beneath

the beam at 30 microns per second during

analysis, The accelerating voltage and beam

current were maintained at 20KV and 50nA

respectively.

TABLE 3

Comparison of the X-ray diffraction pattern of

the Dame Rock mineral with those of lavendulan

and sampleite

T.avendulan! Lavendulan?

Dome Rock San Juan, Chile Sampleite2

dA I dA I dA I

9,20 vs 9.77 100 9.60 100

7.403 w 7.0) 40 6.85 70

6.76 Ww -

4.98 WwW

4.83 Ww 4.87 50 4.73 40

4.60 Ss

4.37 § 4.4) 40 4.30 80

4.17 s 3.89 70

3.50 vw

3.38 vvw

3.24 vvWw 3.23 50

3.18 vVw

3.12 8 3.11 70 3.04 100

3.06 Ww

2.98 vw

2.92 m 2.90 20 2.89 50

2.74 vw 2.76 20 2.80 50

7.69 m 2.69 50

2.61 m

2.47 m 2.48 20 2.50 50

2.40 Vw

2.34 vw

2.24 vvw

2.10 vw

2,02 vw

1.95 w 1.97 20 1.91 50

1,90 w

1.84 9 vyw

1.81 vw 1.83 20 1,79 710

1.75 m 1.76 20

1.72 vw 171 80)

1.69 yyw

1,66 vw 1,61 50)

1.50) yw 1.55 20 gar 70

140 w 1.47 20 1.44

1.42 20 1.37 70

1.21 20 1,21 50

1. Diffraction data measured by J. G. Pickering

(C.$,1.R.0.) using a 19 cm camera and CoKa

radiation.

Diffraction data from A.S.1.M. cards Nos.

11-351 and 11-349,

1 Normal conditions of electron probe microanalysis

Accelerating valtage 20 kV

Beam current S0nA

Flow proportional counters

Counting time: 10.seconds (line and one background position)

Spectrometers: LiF crystal—CnKa, AsKs, CoKa, Caka

Mica crystal—Naka, PKa, ClKe, MgkKa

Beam fully focussed

PHOSPHORIAN LAVENDULAN FROM DOME ROCK MINE 137

The raw output data from the electron

probe were refined by the CDC 3200 computer

program MICANCOR (written by H. Rosser

of C.S.LR.O.), which incorporates the correc-

tion program MKRPRB6 (Oertcl 1971). The

mineral analysis reported in Table 1 is the

average of analyses of eight selected arcas of

the mineral fragments in the polished section,

Results

The X-ray diffraction pattern (Table 3) of

the unknown mineral (measured by J, G.

Pickering) is similar to the diffraction patterns

of the isostructural minerals Javendulan

Na(Cu,Ca) g({AsO,),;Cl4HsO and sampieite

Na(Cu,Ca) ,(PO,),Cl4-5H.O. Therefore a

structural formula was calculated on the basis

of a total of 4(As+P) atoms (Table 2).

The result given in Table 2 agrees quite

closely with the data given by Guillemin

(1956) except for the excess of Cl in our

specimen.

We have used the name lavendulan rather

thun freirinite in accordance with the list. of

New Mineral Names (Fleischer 1957).

References

Baviiss, P.. LawrRENCE, L. J., & Watson, N.

(1966).—Rare Copper arsenates from Dome

Rock, South Australia. Avst. J. Sci. 29(5),

145-146.

Campana, B., & Kine, D. (1958).—Regional Geo-

logy and Mineral Resources of the Olary

Province. Bull. geol. Surv. S. Aust. 34.

Dickinson. S. B, (1942).—The structural control

of ore deposition in some South Australian

Copper Fields, Bull. geol. Surv. S. Aust, 20.

FLeiscHer, M. (1957),—New Mineral Names.

Am. Miner. 42, 117-124.

GuiLtemin, C. (1956)—Contribution a la miné-

ralogie des arséniates, phosphates et vana-

dates de cuivre. 1, arséniates du cuivre. Bull.

Sac. franc. Minér. Crist. 79, 7-95.

McConneie. J. D. C. (1969),—Photachemical

degradation of a silicate in the beam of the

electron microscope. Phil. Mag. 20 (8th ser.),

1195-1202.

OsrTeL, A. C, (1971).—The calculation of re-

sults in __electron-probe microanalysis.

C.S.L.R.O, Division of Soils, Technical Paper

No. 9.

Strvota, J. (1969)—On the evaporation of some

alkali metals during electron probe analysis.

Bull. geal. Soc. Finland 41, 85-91,

SWEATMAN, T. R., & Lone, J. V. P. (1969)—

Quantitative electron probe microanalysis of

rock forming minerals. J. Petrology 10, 332-

379,

RHODACARIDAE (ACARI: MESOSTIGMATA) FROM NEAR ADELAIDE,

AUSTRALIA. Hl. ECOLOGY

BY D. C. LEE*

Summary

LEE, D. C. (1973).- Rhodacaridae (Acari: Mesostigmata) from near Adelaide, Australia. II.

Ecology. Trans. R. Soc. S. Aust. 97(2), 139-152, 31 May, 1973.

Serial collections of rhodacarid mites extracted by desiccating funnels from surface soil

(greatest depth: 4 cm), moss and plant litter, at two sites on the western slopes of Mount Lofty,

overlooking Adelaide, South Australia were studied, as were small collections of rhodacarids from

two sites on the Adelaide Plain.

The presence of two communities of hemiedaphic rhodacarid mites is demonstrated by differences

in the characteristic species of two sites and a significant association into two groups of the species

of one subfamily (Ologamasinae). Population density is higher in the wet, cool winter and where

there is substantial, decomposing plant litter. Variations are demonstrated between some species in

the number of generations per year, the time for occurrences of particular life-history stages and the

sex ratio. It is suggested that species of Athiasella prefer higher nutrient loamy soils, while

Gamasellus is almost confined to low nutrient, sandy soils.

RHODACARIDAE (ACARI : MESOSTIGMATA) FROM NEAR ADELAIDE,

AUSTRALIA. II, ECOLOGY

by D, C. Ler*

Summary

buc, BD. C. (1973).—Rhodacaridae (Acari ; Mesostigmata) from near Adelaide, Australia. 1

Keology. Trans, R. Soe. 8. Aust. 97{2), 139-152, 31 May, 1973,

Serial collections of thodacarid mites extracted by desiccating funnels from surface soil

(greatest depth: 4 cm), moss and plant litter, at two sites on the western slopes of Mount

Lofty, overlooking Adelaide, South Australia were studied, as were small collections of rhoda-

catids from two sites on the Adelaide Plain.

The presence of lwo communities of hemiedaphic rhodacarid mites is demonstrated by

differences in (he characteristic specias of two sites and a significant association into two groups

of the species of one subfamily (Ofogamasinae). Population density is higher in the wet, cool

winter and where there {s substantial, decomposing plant Jitter. Varjalions are demonstrated

between some species in the number of generations per year, the time for occurrences of

particular life-history stages and the sex ratio, It is suggested that species of Athiavell: prefer

higher nutrient loamy soils, while Gamascllus is almost confined to low nutrient, sandy soils,

Introduction

Rhodacarids are mainly predatory mites, and

are most common and diverse in form in

Southern Temperate regions. The present

work formed part of a study on rhodacarids

from the environs of Adelaide, South Australia

(Lee 1970!), Part L dealt with systematics (Lee

1973) and should be referred to for the

authority to names of rhadacarids collected.

Part IIT, dealing with. behaviour, is to be pub-

lished.

Most rhodacarids are hemiedaphic, being

free-living in surface soil, plant Jitter, or in

moss or other plants with a similar growth

form. Some taxa, however, are not hemie-

daphic. Thus, Hydreagama@sus, Litogeamusns,

Parasiliphis, Perisetus and Tangaroellus have

only been found in or near the littoral zone,

usually on rocky shares; Rhedacaropsis has

anly been found in the littoral zone on sandy

shores: Cyrtolaelaps or Eur)parasitus have

generally been collected from bird or mammal

nests or from but caves; Tangaroellus porosus

Luxton has usually been found under the cara-

paces of barnacles; and the two species of

Laelapronyssus have been found closely

associated with flies or termites. Ecological

studies demonstrating more limited habitat

preferences include only non-hemiedaphic

thodacarid mites. Thus. Aydregamasus littor-

dis (G. & R. Canestrini) mainly occurs in

tock crevices in a limited part of the littoral

zone(Glynne-Williams & Hobart 1952, Morton

1954). Rhodacarus and Rhedacarellus are

commoner in the deeper soil layers (i.e. they

are euiedaphic) and are limited to purts of

sampled areas (Sheals 1957, Davis 1963, Wood

1967a, Emberson 19682), Cyrraluelaps and

Euryparasitus are commoner in mammals’

nests that are on the ground and made of moss

(Mrciak, Daniel & Rosicky 1966).

There is a problem in defining precise habi-

tats for ground inhabiting mites, because a

species may occur in strictly limited habitats,

* South Australian Museum, Adelaide. S. Aust. 5000.

Yipr. D.C. (1970)—The taxonomy and general biology of the Rhodacaridac (Acari: Mesostig-

muta). M.Sc. thesis, University of Adelaide, Australia (unpublished).

“Emperson, R. M, (1968)— The Mesosiigmatu of certain coniferous forest soils in Western

Quebec, with a preliminary account of North American Rhoducaridae (Acarina), Ph.D, thesis,

McGill University. Montreal, Canada (unpublished).

144} Dp. Cc.

hut nt Widely differing localities. For instance,

it has heen shown in three different studies char

Rhodacarus roxens Oudemans has a limited dis-

tribution, It occurred only in a limited area jn

minecul suil over iron-stone in grassland ( Davis

19631; in non-calcaveous drift around wu lime-

stone Oulcrop in moorland (Wood 14¥67a}; and

in allvial saltmarsh (Luxton 1967), This type

of distribution for a number of species of mite

led both Davis (1963) and Wood ({967b) to

suxvest that many mite species consist of ecula-

gical races with different demands upon the

environment and therefore occurring in quite

different habitats.

The main aim of the present work was 16

demonstrate whether or not there ure any habi-

(at preferences amongst hemieduphic thoda-

carid mites. [nerdental information on seasonal

fNuctuations. of populations and fifc-histories

Was also sought, Th addition, becuuse species

association was considered in relation to halvitat

preferences, the correlation between taxunomic

affinity and degree of co-existence is discussed.

Four sites were initially sunpled befare two

were selected for serial sampling. The results

of the preliminary sampling from the two sites

that were not sampled again are also given, be

cause they suggest a possible correlution

WelWeen certain genera and environmental

factors.

Methods

Twe cxtraction methods were used: one for

dealing with disturbed “bag” samples collected

throughout a year and the other for undis-

turbed “core samples collected in August.

1. Bag Sampling and Extraction

Soil, down to a depth of approximately 4

cm, and the fitter or moss on it, was scouped

inte a plastic bag with u trowel. The volume of

a sample was about 1280 ml, and was taken

From in area of approximately 250 cm, This

sanple was poured intu an aluminium tube

(14% 40 em) with a wire mesh bottom, which

was placed on uy coarser wire mesh in 4 Cunnel

(diameter of mouth—2?2 cm] leading down

into a glass vial of 75% alcohol, The sumple

was heated from above by a 40 walt electric

light bulb for five days.

Bay samples were collected once a fortnight

for a year (24.1V.1968-23 iv.1969). On each

occasion four samples were collected between

IL am. and 4+ p.m. 2 From the Summit Site

{Sel or S1), and 2 from the Foothills Site

(Fel or Fl)—see appendix, One sumple of

moss on soil and another of plant litter on

soil were taken from each site. A totul of 108

samples weTe collected in the series,

ibe

2 Care Sampling and Extraction

Stee] core samples (5.15 em diameter x 4

cm uepth) were driven into soil covered hy

moss or litter, dug out, and then sealed by a

lid at each end. The volume of euch core was

about 83 ml and from an area of approxi-

mately 20 cm*. The steel cores, without lids,

were inverted On wire mesh in multiple Tull-

gfen funnels, so that the deepest part of the

soil was uppermost, These funncly incorporated

forced draught ventilation to prevent water

condensation, The samples were heated from

above by thermostatically controtled electric

coils to 25° C for 2 days, tollowed by 30° C

for 2 days. 35° C tur 2 days and finally 40° C

for 1 day.

Core samples were only collected on

S.viii.1968 and J2,,ii1.1968, On cach occasion

16 cores were tiken from points evenly spaced

throuvhout cach of 4 plots (S1, $2, FL snd

F2}—see appendix to this paper. Samples from

2 plots (S82 tind F1) were covered hy « suh-

stantial layer of fermenting plant litter, and

the other 2 plots (S1 and F2) were covered

by moss and 4 litle raw leaf litter. A total of

128 core samples were collected in the serus.

Sites

Four siles Werte sampled between the summit

of Mr. Lofty and the coast-line of the Adelaide

Plain, In the appendix, the Summit and Foot-

hills Sites whieh were extensively sampled arc

described in detail, while the Plains and Coastal

Sites Fram which only small collections were

made are given a briefer description, Two plots

at each of the two former sites ure also des-

cribed.

Temperature and rainfall had linear

gradients between the coast and Mt. Lofey: the

former decreasing ond the lattes increasing with

Neurness to the summit. On the other hana, the

Sunimit and Coastal Sites were similar in hav-

ing low nutrient, sandy soils, in contrast to the

higher nutrient, loamy soils of the wo inter-

venient sites. Three sites had a predominately

Jiative Alora, while dhe Foothills Site had an

alien flora,

The sites that were extensively sampled

(Summit and Foothills Sites) included areas

which were elther almost entirety covered by

plant litter or similarly covered by moss, Core

samples were only collected from rectangular

Plots in such Uniforny ures: one moss plot and

one Jitter plot at each of the two sites, On the

other hand bag samples were collected from

larger areas including both plant Iter and moss

patches.

RHODACARIDS FROM NEAR ADELAIDE 14]

RHODACARINAE ¢ : GAMASIPHINAE

143,136 /'60,119

ef Pa

Fae yf \) e.-

te ~ Ww

el aS fh.

eae ve ;

aa i 3 Ly

dk \ f

ee ene i,

Rhodacarus reseus * { \. f

/ oe \ i

ate oad Fa Ne Eveplerius tilamentasus q i

x ;

G alistralicus ott

OF (12/00) fs -

«i G 4

f 1 70,33 87,859 ;

v S

¢ i a

Gamasiphis

K a

’ ' 1 :

m ts wa ’ a a mm

o 6G fornicatus

¢ 324/ 20.8)

“1

as ; ; G, Jenifornicatus ff

4 te: ¢0.0/5,23 é

Antennolaelapns

OGnchogamasus

virguncula

£0,0/ 7,0)

\ 7 ! SESSILUNCINAE

Fig. 1. Species of Rhodacarinae, Gamasiphinae and Sessiluncinae collected during serial sampling,

Dorsal views of adult females, Numbers given under names equal specimens (any stage) from

the following environments: (Foothills Site moss, FS litter/Summit Site litter, SS moss).

142 bD. C. LEE

Geogamasus howardi

0318, 643/41)

OLOGAMASINI

Athiasella relata

695)147/ 52,189

f Axiiassila Jettars “1, OLOGAMASINAE

(503,102 /143,22)

503, 1102/1432 Hiniphis bipala

co,o/s.0)

GAMASELLINI

Solugamasus

mustela

634.7 / 0,0)

Gumaselius

cophinus

¢2,1/97, 9979

Gamaselius

tagardh|

(5,0 /321,300)

Ganiasellus concinnis

(5,6 / 451,302)

i a \

bo . i Acugamasus puncranis i

Ahodacareides minyaspis Agua BSUS PUNETATS VAcugamasus semIpunctatus’,

(0,0/ 2,3) (0.0/9.0) se 29,0 / 1414)

Fig. 2. Species of Ologamasinae collected during setial sampling, For further explanation sec Fig, [,

RHODACARLDS FROM NHAR ADELAIDE

Resalts

|, Species und /orins represented

Preliminary bag samples from Vhe Plains and

Coustal Sttes in May and June, 1965, produced

the following thodacarids (number of speci-

mens in parenthesis): Plains Site—Rhedacaruy

rosews (18), Gamasiphis australicuy (4),

Athiasella dentata (29); Coastal Site—CGarmua-

sellus grossi (13), Acugemasus elachyaspis

(8)- lt would have been valuable to have pro-

ceeded with scrial sampling at these two sites,

bul becuse of a time limitation this was only

done at the two other sites which supported

more thodacarid species.

Sizes and collection dates of preliminary

samples from the Suramit and Foothills Sites

were not comparable with thase of the other

two siles and are theretore nor Jisted, Serjal

samples from the Summit and Foothills Sites

produced twenty-two species of rhodacarids

(Figs. i, 2), A female Rhadaearetlus silestacas

was listed (Lee 1973) from the Foothills Site,

but this was taken while collecting miles alive

for laboratory cultures. Such collections other-

wise only included species taken in serial

samples.

Only a small proportion of immature chudi-

carids were collected, The 3 species for which

Tesulls are presented (Figs. 6, 7) produced it

relatively high pruporlion of these stages,

Further comments on immature siages are

mide below under Section 5 (Seasonal Varia-

tion),

The sex ratio (male/female) of the 12

commonest rhodacarids From: serial samples is

as Follows; Gamasiphis fornicatus, 0,26: Acu-

gumiasiey . semipunciatux, 0.33, Geegamasus

mininins, 0.344 Geogantasus howarel, 0.41;

Gamasiphis saccus, 0,45; Gamasellus cephians,

0.56: Gamasellus concinius, 0.66; Antes

nolaelaps celex, 0.67; Gamasellus tragardhl,

0.73: Athiasella dentata, 0.83. Euepicrius fila-

meitosus, 0.845 Arhiasella relate, 1.23.

2. Differences between sites

Numbers of specimens were as follows;

Summit Site, 2784 (baz samples, 2)37: core

samples, 647); Foothills Site, 3340 (hag

sumples, 2707; core samples, 633}.

Number ef species were as follows; Summit

Site, 20; Foothills Site, 15. The majurity (13)

of species were foun at both sites, but there

was a considerable difference in the curmpusi-

tion of the fauna. ‘Ihis difference is demon-

straled by presenting the dominance anu fre-

quency of the 12 commonest rhodacarids (Figs.

3, 41. Dominance is the percentage of the total

143

specimens that belong to a species, and is rep-

resented by the size of a shaded urea in a

collimn. Frequency is the percentage of samples

in which a species was found, and is represen-

led by the nuribers in the centre of a shaded

area. Different species are characteristic (i.e.

the most dominant and frequent) of different

sites,

3. Differences between soil cover ef liter

compared with moss

Numbers of specimens were as. follows:

litter, 3558 (bag samples, 2696; core samples,

862). moss, 2566 (bag sumples, 214%; core

sainples, 418). A similar indication is given if

the results from the core samples alone are

expressed as rhudacarids/m? as follows; Sum-

mit Moss Plot, 3450; Summit Litter Plot,

AS60; Fuuthills Moss Plot, 3080; Poothills

Litter Plot, 6310.

Numbers of species from Summit and Foot-

hills Sites were as follows: fitter, 21; moss, 19.

The majority of species (18) were found in

both litter und moss-covered soil. Comparing

the dominance and frequency of individual

species (Figs. 3, 4) it is evident that the species

composition of a particular site is simiar

whether it is cavered by litter or moss. ‘The

preatest differences are shown by the core

samples when the whole plot was mainly

covered by cither litter or moss. Some species

show distinct preferences: e.g. Athiasilla den-

sate for litter; Gamasellus coptinus for moss.

On the other hand. a preference at one site

muy be apparently reversed at the other site,

e.g. Geogamasuys minimis

4. Species Association (only Qlogamusinae)

Exch site has dWferent characteristic species

(see Section 2), mainly belonging to the

Ologamasinae. To eslabhsh whether or not two

communities ate present. the significance of

associations in samples between species of

Ologamasinae is examined. I have followed

Dvebauche (1962) in usin o correlation co-

eflicient based on 4 contingency chi squared

test us a measure of degree of association or

dissociation of species.

The correlation coeflicients fron the results

of bay samples (Table 1) produce the clearest

pattern, Of the 28 terms, 18 ate significunt at

the 1% level or Tess, ‘The species fall into two

groups. One group (afhinselfa dentata and

others) includes species characteristic of the

Foothills Site. The other group (Geagiurasis

tninimus and others) includes species charjc-

teristic of the Summit Site. Since Adhiasella

dentate and A. relata regularly occur al both

ea)

dD.

144

—

“

Footwits Summir Summit

Foothills

Species

(Sci+51)

CFci#Fy)

Bhis

Gamasi

is}

25959 Rs

OG,

rats

Phis

Garnasi

Hews

rts oe ky ser fctoeevi re

[damentasus

FuepiéHns

entat

howard

Athiaseua

Geogamasus

asus

gam

Geo!

minimus

Gomusellus

sconcinAus

Samasetlus

ophinus

Gamaselius

eee

jamasus

Acuy

punctatus

semi

Olaelaps

Antenn

rhodacarids

eclox

Orher

odacarids in bag samples

—

= 9

oo =

=n]

=m)

=i)

Laney

cal

The dominance and frequency of the |

(collected from 2 sites throughout th

145

RHODACARIDS FROM NEAR ADELAIDE

CORE SAMPLES

Summit ‘Summit

Foothills

Moss

rornicatu

Gamasiphis

seccus

pPicrius

Gus

filarm

dentata

Arhiaselia

Athliasella

pS eg Estes ar

aS ce sierra oer STEEISET

eoeeoenee_eetaes ee #ee s® ¢

e_e © 2 68 «Pe eee ee eee Oe

Geogamasus

Geagamasus

minimus

Gamasellys.

SOnclany

Gamasellus

cophinuss:

none

Gamesseltu

Acugam.

elaps

Antennola

chnodacsrids

f thodacarids in core samples

the dominance and frequency of the 12 commonest specics o

Fig, 4.

anation see text.

(collected from 4 plots it early August). For further expl

146 D. C. LEE

TABLE 1.

Correlation of Ologamasinae species in 108 bag samples containing 4,844 specimens.

Correlation indices (C X 104), +> (association) .— (dissociation), upper limit is 707.

Species A.den. A.rel. Gow. G.min, G.cop,. G.con. Gira. Asem.

Athiasella dentata +355 +448 —49 —142 —256 —197 —36

Athiasella relata (EY +307 iY) +57 —32 —4$ —t4

Geogamasus howardi Corey ES ee) —319 —495 —583 —S566 —299

Geogumasus minimus 0 0 (4/7) _ +517 +394 = |399 +58

Gamasellus cophinits 0 (///) Cet) +580 +598 +287

Gamasellus cancinnus (f//) 0 (f///) (PFti eer} +656 +396

Gamasellus tragardhi — 0 (//1) (FR) CeRRY (Fea) CR)

Acugamasus semipunctatus ( 0 /f) 0 (ca a Gina +349

Significance of relations:

None Positive Negative

P> 0,1 0

P< 0:1 + =

P< 0.01 (**) (//)

P= 0.001 (ar G//)

the Summit Site as well as the Foothills Site, (Arhiasella dentata—Garnasellus cophinus,

there is, in the main, only a significant dissocia-

tion between Geogamasus howardi und species

al the Summit Site.

The correlation coefficients from the results

of care samples (Table 2) are similar to those

of bag sumples but with 1 drop in significant

associations. Of the 28 terms, 12 (6 associa-

tions, 6 dissociutions) are significant at the 1%

level or less. Although there are the same num-

ber of significant dissociations, 3 are for dif-

ferent pairs of species. The reduction in

associations is only significant where a pair of

species was either uncorrelated or significantly

associated in bag samples while being signifi-

cantly dissociated in core samples. This was

true at the 1% level or less for three pairs

Athiasella dentata—Guamasellus tragardhi, Acu-

gamasus semipunctatus—Gamusellusy Concin-

nus). Such a significant dissociation in core

samples could have had a number of causes:

smaller sample size isolating niches; sampling

separate moss or plant litter covered plots (one

at each site was outside the area used for bag

sampling), thus isolating niches and possibly

introducing new ones: fewer mites per sample;

no seasonal effects such as the absence of any

rhodacarids [rom mest summer samples. The

conspicuous change in dominance between bag

and core sampling of Acigamasus semipune-

ratus In “Foothills moss” samples and Gama-

selius trragardhi m “Summit litter” samples sug-

gests that the significant dissociation in core

TABLE 2.

Correlation of Clogamasinue species in 128 core samples containing 1,280 specimens.

Correlation indices (C X 108), + (association), — (dissociation), upper limit is 707.

Species a.den, A.rel. G.how. G.min, G.cop. G.eon. G-tra. A.semi.

Athiasella dentata +355 +369 —i06 —3&2 —24 —327 —205

Athiayella relata Soaiea | +10 +49 —85 +87 —156 —35

Geogamasus howardi (*#*) 0) =—344 —309 —418 —203 +30

Geogamasus minimus 6 0) (///) +213 +322 +161 —If6é

Gamasellus cophinus (///) 0 f/f) = +264 4236 —102

Guamayellus corcinniy 0 0 (///) (+#*) (er) —20 —231

Gamasellis tragardhi (///) —_ _ + (F*) 0 4355

Acugamasus sermipunctatus _ 0 0 — 0) (//) (**)

Significance of relations:

None Positive Negative

P> 0.1 0

P< 0.1 + —

P< 0.0L (#* (fA

< 0,001 (*??) (//1)

RHODACARIDS FROM NEAR ADELAIDE

samples of the above pairs including these

species is due to the difference in arcas

sampled. The same cause may apply for the

dissociation between Athiasella dentata and

Gamasellus caphinus.

Seasonal Variations

Seasonal fluctuation in total numbers of

rhodaearids at each site based on bag sampling

are summarised in Fig. 5. There was a con-

spicuous fall in numbers of rhodacarids in

samples collected during the summer (Decem-

ber-February). This is associated with a drying

out of the environment and rainfall figures for

Stirling (5 km SSE of Summit Site) are given

as a factor closely associated with this process.

The low number of samples taken means

that seasonal differences indicated for the two

147

sites are tentative. The number of rhodacarids

from the Summit Site was fairly constant

throughout the wetter months (May—Novem-

ber). At the Foothills Site the rhodacarid

population apparently gradually increased in

September and October to a peak, which was

nearly twice the highest number at the Summit

Sitc. If this change is true for the actual popu-

lations it could be telated to the dominant

genus at the Foothills Site, Arkiasella, being

multivoltine, while abundant species at the

Summit Site are univoltine (see below).

Seasonal fluctuation in numbers of the dif-

ferent developmental stages and sexes of

Gamasellus concinnis, Gamasellus tragardhi

and A thiasella dentata are represented by histo-

grams (Figs. 6, 7). Not enough immature

APR MAY JUN Jui AUG sep oct NOV DEC JAN FEB man APA

T 1 | | ] ‘ftw TT T T T

ts a RHODACAAIDS COLLECTED eee

TOTAL pe M--aAT FOOTHILLS SIE —t3a0

|— @--ar SUMMUT SITE hae

NUMBER L. a / ao

- . ™ 150

7 /

OF . s a 5

|__ a7 fod

ae \ / on e"-8 a

a Ll s A

fo N x bd

s—a— By a a“

BMECIMENS L. e ‘~,—s 0

‘\ / \

= \ } e PY 150

e ae \

to e—e-* s a \ va \ ran

Jf ‘ ) ‘ a o.

s— 6. at}

— e Na \ 50

X s—e_

i o—*_, ~e fs

RAINTALL AT STIRLING ¢ NEAR SUMMIT SITE)

+ #.—-AcTUAL FORTNIGHTLY fA.

| » oy. O---AVERAGE MONTHLY B

Z me

* "Y=

|. y, ee 7,

& [4 eo +

|_ > a

RAINFAL | 4 “sO

“¢ ys,

2 ke af

+ \ ss

IN - \

a , \o

’ 4 bares

“ ls r he re

im 9oNY -~ vo ot)

o L_ + + + \

th ft, =I. | Le al | |

TIME

OF ‘YEAR

Fig, 5. Scasonal fluctuation in numbers. of Rhodacaridae collected in bag samples at two sites during

1968 and 1969. Rainfall records are for nearby Stirling.

148 D.C, LEE

stages of the other rhodacarid species were col-

lected to warrant presentation here.

In Canada, where the winter is extremely

cold, Gameasellus vibrissatus (which is mor-

phologically very similar to G. iragardhi) over-

winters as adult females which give rise to a

single generation in the following summer

(Emberson—footnote 2). My results show that

Gamasellus tragardhi (Fig. 6) bas a similar

life history, except that it over-summers as

adult females and males which give rise to a

single generation in the following winter.

Gamasellus concinnus (Fig. 6) is also univol-

tine, but over-summers in the deutonymph

Stage, the males emerging before the females at

the onset of the wet season, Arhiasella dentata

(Fig, 7) probably over-summers in the adult

stage and it breeds for a longer period, prob-

ubly being multivoltine. Results for some other

species (Lee—footnote 1) are inadequate but

suggest the kind of life-history that they have.

Geogamasus towwardi, Athiaxella relata and

Euepicrius filamentosus appear to have similar

life-histories to Athiasella dentatu. Gamasiphis

vaccus and Gamasellus cophinus may be uni-

voltine and over-summer in the egg or early

immature stages.

It is noteworthy that the life-histories indi-

cate that there are large numbers of rhoda-

carids (e.g. deutonymphs of Gamasellus con-

cinnus) in the soil during the summer that

were not represented in the samples considered

here, Possibly they moye down deeper than the

surface 4 cm sampled. There is no clear indica-

tion that rhedacarid species stagger their life-

histories so as to avoid exploiting the environ-

ment concurrently.

Discussion

The twelve commonest. species of rhoda-

carids in serial samples were found at both

Summit and Foothills Sites, but each site had

ee a y

GAMASELLUS CONCINNUS GAMASELLUS TRAGARDHI

[ FEMALE

i oo

zie

a a MALE

I 7. DEUTON.| is ss

ints

Ee ls ad atrnnd oma Ae tae dans PROTON. eo oh) 79 35 (Eom: oe

ato eb

APH IMAY! JUIN | JUL) ALS! SER Oct NOY! DEC! Jan] Pea) Man) APR

SE POR VTE ! gba tbat a |

APRIMAY | JUN [JUL | AUG) SEP OCT NOV |DEC. JAN LFEBIMAR APR/

Fig. 6. Seasonal fluctuation in numbers of individuals at different developmental stages of Gamasellus

concinnus and G, tragardhi collected in bag samples at two sites during 1968 and 1969.

RHODACARIDS FROM NEAR ADELAIDE 149

= frmale

oe Mate

BEUTON,

‘aL,

3|.

an PROION

mom [tanya

A On sO On

APA MAY ALM dol pale SFP Oa|NoY, Jeo inn Poe lmAR Apr

Fig. 7, Seasanal fluctiation in numbers of in-

dividuals at diferent developmental stages

of Athfasella dentate collected in bag

sanupiss at two sifes duting 1968 and

1969.

different characteristic species and amongst

members of the Ologamasinae there was a

highly significant association between species

characteristic of a site, thus demonstrating the

presence of two rhodacarid communities,

Because serial samples were only taken from

two sites (Summit and Foothills Sites). and

environmental factors were not measured, it is

impossible to confidently associate the rhoda-

carid taxa with particular factors in the envir-

onment. If, however, the few samples from the

Plains and Coastal Sites are considered, there

appears to be a similarity between the rhoda-

carid faunas of the Foothills and Plains Sites,

in that Arhiaselia had the biggest representa-

tlon, and between the Summit and Coustal Sites

in that Gamesellus had the biggest representa-

tion. It appears, therefore, that the coastal sand

dunes as well as the low nutrient, sandy soils

near the summit of Mount Lofty are favour-

able to Garnayellus while the higher nutricnt,

loamy soils of the foothills and plain are not

favourable. The converse appears to be true

for Athiasella. Factors such us temperature and

tainfall, which have a linear gradient between

the coast and the summit of Mount Lofty, do

not appear to be directly favourable or un-

favourable to particular taxa. Tt is noteworthy

that although the flora at the Foothills Site was

introduced, mainly from outside Australia, the

gamasine fauna was predominantly rhodacarid,

with characteristic species that are probably all

eidemic to South Australia and belong ta

genera probably endemic to Australia,

Although the composition of the rhoducatid

fayma of a particular site was similar in soil

samples covered by litter and those covered by

moss. a few species showed a distinct prefer-

ence for one or the other habitat, Other

attributes revealed for certain taxa were the

iendency for species in the same genus to have

similar scx ratios and the specics of one genus,

Gamasellus, to follow quite different life-

histories.

Species of some genera (Arhiasella and

Gamasellus) were characteristic of one site,

while for other genera (Geogarnasus) this was

not true. Conflicting hypotheses on species

association were resolved by Bagenal (1951).

who stated that “related species are more likely

to be found in similar, though not identical,

habitats than are unrelated ones”. Hurlbut

(1968), working on species belonging to

families closely allied to the rbodacarids,

reached a similar conchision expressed as

“species which are very different anatomically

or very similur anatomically coexist less often

than species which are moderately similar to

each other’. Certainly the three species of

Gamaselluy associated at the Summit Site are

as dissimilar (see Fig. 2) from each other as

it is possible to select from known species of

Gamasellus and would probably be considered

by Hurlbutt (1968) as ‘moderately similar’.

They must exploit different ecologtcul niches

within the volume of the small cores in which

they were cqilected. The same is likely.

although not so clear-cut for the two species of

Athiasella,

The very slight but easily discernable mor-

phological difference between Gamuavellus tray-

ardhi from the Summit Site and Garmasellus

grossi from the Coastal Site (Lee 1973) sug

gests that the level of taxonomic distinction is

closely associated with ease of anatomical diap-

nosis rather than genetic similarigy. The

Rhodacarus specimen from the Summit Site is

possibly equally dissimilar to the Rioducaruy

specimens From the Plains Site (Lee 1973).

both ef which I have refetred to R. rosens, 1

suspect that many mite species which show

limited distnbution in widely differing geo-

graphical locations (see Introduction) are also

grouped in one species because of difficulties

in diagnosis,

D. C LEE

Acknowledgements

Tam indebted to Dr, K. E, Lee for the use

o£ Tullgren funnels at the Soil Zoology Section

of the C.S.LR.O. Soils Division, and for his

comments on this manuscript, I also acknaw-

ledge the helpful advice afd criticism received

from Dr. D, A, Duckhouse, University of Ade~

laide, during the preparation of the M.Sc, thesis

which formed the basis of this study,

Lam most grateful to Mrs, Curol Aitken for

Preparing some drawings (Figs. 5-7) and to

Mrs: Brenda Head fer preparing the other

drawings (Figs. 1-4) as well as to Mrs, Jo

Bramley and Miss Debbie Rankin for carefully

typing the manuscript.

References

RagewaL, T. Bo 19511—A note on the papers

of Elton and Williams on the generic relu-

lions OF species in smal! ecological com-

munities, f, Anim, Ecol. 20, 242-245.

Dayis, B. N. K. (1963).—A study of micro-

anhrepod communities in mineral soils near

Corby, Northants. J. Anim. Ecol. 32, 49-71,

Denaucnr. Hy R. (1962).---The structural analysis

of Animal Communities of the soil. Jy PW.

Murphy (ed,}, “Progress in Soil Zuvlogy". pp,

16-25. (Butlerworth: London, }

GLYNNE-WILLIAMS, J, & Hopart, J. (1952),—

Sludievs on the crevice fauna of a selected

shore in Anplesey. Prov. 200! See. Lond.

L22, 797-824.

Nurteure A.W. (1968), Coexistence and atia-

tomical similarity In two genera of mites,

Veigala and Asca. Syst, Zoal, 17, 261-27).

| ke, BD, C. (1973)—Rhodacavidae (Acari: Mesas-

tigmats) from near Adelaide, Ausiraliu, 1.

Systematics, Ree. §. Aven Aldus. 16 114), I-

af.

liicHrienp, W, H. (1960).—Soitly on the western

Slopes of the Mt. Lofty Runge near Adelaide

and Elizabeth, South Australia. Divi Rep. Div.

Swils CSIRO 8/59, 1-36,

Luxvon, M, (1967)—The Zonution of Saltmarsh

Acarina, Pedobiolagia 7, 53-6,

Morton, J. E. (1954)—The crevice faunas of the

Upper intertidal zane yt Wembury. J. mar,

bivl, ayy, U.K. 33, (87-224,

Meciak, M., DanteL, M. & Rosicky, B. (1966),—

Parasites and nest inhabitants of small mam-

mals in the western Carpathians, 1. Mites of

the superfamily Gamasoidea (Purasitiformes),

deta Fac, Rerum nat. Waive. eomen.. Brarist.,

Zook 13. 81-11.

SHeaus, J. G. (1957)—The Collembola and

Acaring of uncultivated soil, J. Anin. Eeol.

26, 125-134.

Sencar, R.L.(1972).—"The vegetatinn of South

Australia’. (Government Panter: Adelaide, )

Server, R. £,, & Perey, R, A, (1948).—The

Plant ecology of part of the Mount Lofty

Renaes (1). Troe. Ro Save. 8. Aust, 72, 91-

132.

Woop. T, G. (1967a).—Acari and Collembola of

moorland, soils from Yorkshire, England. |.

Description of the sites and. their populations,

Oikos 1B, 102-117.

Woon, T. G. (1967b).—Acari and Collembola of

moorland soils from Yorkshire, England. 1.

The micro-arthropod communities. Oikey (8,

277-292.

Appendix: Details of Sampling Sites and Plots

Summit Site, Locations Mi. Lofty, near ta sum-

mit, approx. 18 kin trom the sea, Australian Map

Grid vo-grdinales: 290600 nv E/61272320 m N,

map fo. 6628-48-j, Dept. of Lands, Adelaide.

Height above sea level: 640-670m. Rainfall: mean

annual vaintall approx. 120 cm; figures osed in

graph (Fig, 5) are for Stirling (5 km SSE of

site) with a man annual rainfall of 119.0 cm,

and 4 total rainfall in 1968 of 161.6 cm; it should

be noted thal “a large percentage of soinfall is

lost to the soil by run-off an the Adelaide Hills”

(Specht & Perry 1948). Temperature’ mean

monthly min./max, temperatures for Stirling are

January, 11.5°/24.5°C; July, 4,5°/10.5°C. “Ver-

rdiny steep western slope of hill, near to summit,

Soil: Black Hill Assoclation—“low nauicient re-

server im most Soils in Which shallow depth is the

chief limiting physical churacteristic’ (Litchtield

1960); shallow (10-35 em}, dark grey, loamy

sand; an analysis of soil fram Mit, Lofty Summit

showed 0.004469 PO; und 0.0405 Nitrogen

(Specht & Perry 194%). Vegetation: open-forest of

Stringy Burk—Ficwalypiws obliga LoHérit.—with a

sclerophyllous understorey of small native heuth

shrubs including Banksia ornatr FVM. ex

Meisn., EZpucris dipressa Labill. and Leptosper-

mum juniperinum Sam, Fifteen other species of

native shrubs. herhs or grasses were collected from

the site.

Ceneral Snmmreit Plot (Sel). A sub-thombaid

RHODACARIDS FROM NEAR ADELATDP 1S]

area (approximaely 1% a 12 m) which ¢on-

sliluled @ clearing ymanast charred trees with

q draingge channel ronning through the centre

A fire had passed through the plot three years

before (February, 1966). The eastern half of

the clearing had substantial vegetation, includ-

ing abundant fireweed—Sacielia achilleoides

R. Br. ex Ait. a sheart-lived, “high-fertilily-de-

manding” species depending on the temporary

rise in fertiliiy-level due to the ashes of the

burnt vegetation (Specht (972). The western

half of the clearing bad 9 sparse vegetation of

heath shrub seedlings and extensive patches of

moss. Plant Hitter was almost absent from the

mossy half of the clearing, but had wecumu-

lated as raw leaves and twigs around the bases

of tree slumps. Fallen branches and smail shrubs

in the other half, Bag samples were collected

from this plot.

Sammit Moss Plar (Si). A rectangulur area (2

x 10 mj lying approximately at the centre of the

western half of plot Sel, Covered alniat entirely

by on mat of moss. All core samples, and after

August some of the bag samples. were collected

fram this plot,

Summit Liter Plot (S2), A rectaneular area [2

x 10 m) lying approximately 20 m casi of plat

Scl. and separated from It by a bilamen toad,

No fire had been through the plot for 25 years.

Understorey Was thick with heath shrubs und

decomposing plant litter (mainly 1.0 cm deop)

covered most of the ground, Only care samptes

were collected fram this plot,

Foorhills Site, Location: Foothills of My. Lofty.

approx, 16 km from the seu. Australian Map Grid

co-ordinates: 288230 ot E/4127620 m h, map no,

628-49-e, Dept. of Lands, Adelaide, Hetght above

seo level; 240-270 m. Ruinfall: mean annual rain-

fall is appros, 94,0 cm. Temperature; mean

monthly min,/max. temperatures for Glen Osmond

(§ km W of site) ave January, 16°/28°C; July,

7° ¢1S°C, Terrain: hattom of steep northern slupe

(south-Facing aspect of ridge] of Waterfall Gully,

just west of First Waterfall, beside an artificial

pond formed by dredging and damming First

Creek, Soil; Osmond Association—“Nutrient te-

Serves presumably intermediate hetween

law levels ... and the moderate levels in the red

brown carthy af the piedmont aprons” [Litchfield

1940): shallow ta deep (35-110 cm), allavial red-

brown loan, artificially mieved to present position,

possibly from creek hed. Vegetation: alien {is it

mainly i& on bottom 15-20 m of slope downstream

from this point. further up slope from site there

are Manna Giums—Encalypris virinelis var,

huheriana (Naudin) Burbridge-and Drooping

Sheoaks—Caxaerina stricta = Ait}; Fan-leaved

palms (i.fvistonia sp.), Olives (Olea europaea L.),

Lilacs (Syringa wileari« L.) and Fitfesperim (tn

fiefarien Vent, (native of eastern stutes); under-

storce of brambles, bracken und live species of

herhs and grasses; only native plant found was a

small hetb—Gerunium pilosan| Forst,

Gereral Foothills Plor (Fetj. A sub-rectanga-

lar area (approx. 20 © 8 m) which constitited

a patch of quile thick alien vegetalion on the

north bank of the pond, Although the bunk was

steep, the understorey held the plant toec in

nest places. but where the hank was very sleep,

or the ground stony, there was lillle or no

litter and moss or liverworts grew. Bag samples

were collected from this plat.

Foothills Litter Plot (F1). A rectungular urea

(2 © 10m) tying spprex, at the centre of plot

Fel. Covered by plant litter (Olive leaves. pre-

dominated, mainly 2.0 em deep) and some

herbs and eruss tussocks. All core samples, and

after August same of the bag samples, were

collected from this plot.

Foothills Moss Plot (P21, & rectangular qred

(2 x 10 m) lying approx. 10 m west of plot

Fel. und separste! from ic by si artificially

channelled creek bed. Which was stecp and

usually dry. Some soil bare but mostly covered

by moss or liverworts. Under a row of snaall

trees (Pitresporam endalitem) evenly planted

along the west bank ot the creck. Only core

sumples were gollected from this plot.

Plainy Site, Location: Heywood Park, Unley. an

the Adelaide Plain, approx. & km from the sea

Australian Map Grid co-ordinates: 280810 m

E 6128350 m N, map no 6628-50-e, Bem of

Lands, Adelaide, Height above sea level: 30-A0 m-

Rainfall: approx: 38 cm/yeat. Tensperature:

January. [6.4°/29.8°C, July, GS /I45°C, Ter-

rain; small, flat suburban park, wilh fall frees sur

rounding clearing, Sojl; Edwardstoawn Association;

red-brown loum. Vegetation: savannah woodland

of River Red Gums—Encotyptus camatdulensis

Dehnh—"is confined to grey-brown podsols on

jhe slopes and ridges and alluvial soils in the

valleys, both soils being rich in PaO; and nitrogen

and having high water relations” (Specht & Percy

1948): understorey of grass amongst patches of

Fuculyprix liter, Samples fram patches of litter

under River Red Guo.

Coastal Site Location: “Pinery”, Grange Golf

Course, near cost of Adelaide Plain, approx, 1.3

km from the sea, Ausiralian Map Grid co-or-

dimales; 271910 m E/6137D40 m W, map no,

6528-36-m, Dept. of Lands, Adelaide. Height

above sea level: #30 m Rainfall; approx, 43

em/yearm “greens” artificially watered. Tempera-

jure; January, 19°/28°C: July 6.5°/15°C Ter-

rain! inland relicts of coastal dunes formed in

Pleistovene Period, modified to .a golf course. Soil:

Osborne Association; calcareous sand in which the

soluble calcium bicarbonate has been leached to

lower horizons. Vegetation; low woodland of

Native Pines—Callitris preissti Mig.—-with under-

storey of mioss and sparse grase, on dune ridges,

amongst artificial grass wreens; “a “degraded”

climax plunt community characteristic of infertile.

fien-calcareous, sandy snifs” (Specht 1972),

Sumples from mots mats under Native Fines,

ase 31 AUGUST, 1973

TRANSACTIONS OF THE

INCORPORATED

CONTENTS

Watson, Jeanette E. Pearson Island Expedition 1969—9. Hydroids - el 5S

Burn, Robert Pearson Island Expedition 1969—10. Opisthobranchs_ - - 201

Seed, W. F. Pearson Island Expedition 1969—11. Crustacea: Isopoda rey,

Daily, B., & Milnes, A. R. Stratigraphy, Structure and Metamorphism of the

Kanmantoo Group (Cambrian) in its YER Section East of

Tunkalilla Beach, South Australia - - - 9G Pails}

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

—— ee eee we Doe

PEARSON ISLAND EXPEDITION 19697-9. HYDROIDS

BY JEANETTE E.. WATSON*

Summary

WATSON, JEANETTE E. (1973) . -Pearson Island Expedition 1969.-9. Hydroids. Trams. R.

Soc. §. Aust. 97(3), 153-200, 31 August 1973.

Intensive collecting of the sublittoral hydroid fauna of Pearson Island in the Great Australian Bight,

in January, 1969, yielded 81 species (with 3 varieties in one species), of which 13 species are newly

described. There are 18 new records for South Australia and 1 new record for Australia. The

collection permits a fuller description of seyeral hitherto poorly known southern Australian species.

Collections were made using SCUBA at 3 localities representative of environmental extremes on

the coastline-a rough-water site exposed to prevailing swell, a sheltered embayment, and a deep

water situation in open ocean.

The deeper water fauna contained species already known from deep dredgings in the

Great Australian Bight, but differed markedly from the collection from shallower water, with only 1

species common to both.

The Sertulariidae and Plumulariidae are represented by the greatest number of species, and are

equally abundant in both epizoic and epiphytic habitats; the Haleciidae, Lafoeidae and Syntheciidae

are epizoic, and Lineolariidae, with 1 species, epiphytic. The large plumose colonies of the

Aglaopheniinae are epilithic. Hydroids are more abundant on the rough-water coastline, where red

algae and the solitary ascidian, Herdmania momus (Savigny), are epiphytised by a large number of

species. Delicate athecate species, and species of the Campanulariidae which may be expected to

liberate medusae, are restricted to sheltered waters, or to depths below turbulence from surge in the

rough-water locality.

The high percentage of hydroids now known to be common to the coasts of South Australia,

Tasmania and Victoria, supports the view that the Flindersian proyince extends from Bass Strait

into the Great Australian Bight,

PEARSON ISLAND EXPEDITION 1969+—9. HYDROIDS

by JEANETTE E. WATSON*

Summary =~

Warson, Jxanetre E. (1973)—Pearson Island Expedition 1969,—9, Hydroids. Trans. R,

Sec, 8. Aust. 97(3)_ 153-200, 31 August 1973.

Intensive collecting of the sublittoral hydroid fauna of Pearson Island in the Great

Australian Bight, in January, 1969, yielded #1 species (with 3 varietics in one species), of

which 13 species are newly described, There are 18 mew records for South Australia and 1

new record for Australia. The collection permits a fuller description of several hitherto poorly

known southern Australian species, :

Collections were made using SCUBA at 3 localities representative of environmental

extremes on the coastline—a rough-water site expased to prevailing swell, a sheltered embay-

ment, and a deep wuler situation in open ocean.

The deeper water fauna contained species already known from deep dredgings in the

Great Australian Bight, but differed markediy from the collection from shallower water. with

only 1 species common to both,

The Sertulariidae and Plumoulariidae are represented by the greatest number of species,

and are cqually abundant in both epizoic and epiphytic habitats; the Haleciidae, Lafoeidae and

Syntheciidae are epizoic, and Lineolariidae, with 1 species, epiphytic. The large plumose

colonies of the Aglaopheniinae are epilithic. Hydroids ar¢ more abundant on the rough-water

coustline, where ted algae and the solitary ascidian, Herdmania maomus (Savigny). are

epiphytised by a large number of species. Delicate athecate species, und species of the Cam-

panulariidac which may be expected lo liberate medusae, are restncted to sheltered waters. or

to depths below turbulence from surge in the rough-water Jocality.

The high percentage of hydroids now known to be common to the coasts of South

Australia, ‘Tasmania and Victoria, supports ihe view that the Plindersian preyince extends

from Bass Strait info the Great Australian Bight,

Introduction

Hydroids have been reported from a num-

ber of expeditions around the southern and

south-eastern Australian cOastlineé—the yoyage

of the “Rattlesnake” (Busk 1852), the “Chal-

lenger” dredgings in Bass Strait (Allman 1883,

(884), the “Thetis” dredgings along the New

South Wales coastline (Ritchie 1911). the

“Findeyyour” expeditions from New South

Wales to Western Australia (Bale 1914, 1915),

the Michaelson-Hattmeyer Expedition to

Western Australia (Stechow 1924, 1925}, and

the McCoy Society Expeditions to Lady Julia

Percy Island, Victoria (Blackburn 1937), and

the Sir Joseph Banks Group, South Australia

(Blackburn 1938). With the exception of the

last two expeditions, the hydroid collections

were made over a wide geographical area,

while the collections of the Michaelson-Hart-

meyet Expedition and the McCay Society Ex-

peditions, although restricted in urea, were

gained mainly fram drifi, the eulittoral zone,

and to a minor extent, from shallow subtidal

dredgings. No intensive survey has. however,

been made of the subtidal hydroid fauna at

any one locality in the Australian region,

The joint expedition of the Department of

Fisheries and Fauna Conservation of South

Australia and the Royal Society of South Aus-

tralia to Pearson I, 6-15 January, 1969, pro-

vided an opportunity to undertake a compre-

hensive subtidal survey of the hydroid fauna of

an offshore island.

“Honorary Associate, Invertebrate Zoology, National Museum of Victoria, Melbourne, Vic. 3000.

+ Other accounts of the geomorphology and biology of the Pearson Islands are given in Volume 95,

Part 3 (4971) of the Transactions, as well as in the present part.

1%4

The South Australian hydroid fauna is

known from reports of the ‘‘Endeavour™

dredgings in the Great Australian Bight along

the 126° parallel of longitude, together with a

small collection from the Isles of St. Francis

in the Nuyts Archipelago, Blackburn (1938)

recorded the shallow water fauna of the Sir

Joseph Banks Group in Spencer Gulf, and

Shepherd & Watson (1970) listed and dis-

cussed the associations of hydroids and algac

at West 1., Encounter Bay.

The survey yielded a total of 81 species

(with 3 varieties in one species), of which 13

species ate new; there are 18 new records for

South Australia, including { new record for

Australian waters. Only 2 athecale species

were found, and 6 of the thecate hydroids

could be identified only to genus.

Pearson I. (Fig, 1) is:a graniuc island situ-

ated ai Lat. 33°57'S, Long. 134°15'E. about

—

shelfered site

roar

Eastern Cove

Lang J34° 15'E

Lot 33° 5a! go"s

NORTH SECTION

Harte

wf aval

SECTION

2 409 8

metres

Fig. 1. Map of Pearson Island, showing study

sites near the northern cnd. Inset shows

the situation of Pearson Island in the

Great Australian Bight. (After Shepherd

& Womersley 1972).

IRANETIE &, WALSON

64 kim offshore on the continental shelf in the

eustern fegion of the Greut Australian Bight,

Weatheritig of the granite has produced a

rugged Lopography of massive blocks, cletts

aud caverns, continnous to the seafloor at

depths of 45 m immediately surrounding the

island, with a rapid increase in depth offshore

to 70 m. A more detiled account of the en-

vironmental conditions is given by Shepherd

& Womersley (1971),

Methods

Collections were mude by divers using

SCUBA. As diving time was limited toa total

of 30 hours underwater, two main sites were

chosen for intensive collecting. One site wus

on the rough-water windward, southwesterly

side of the island; the other was in the more

sheltered north facing Eastern Cove (Fig. 1),

The benthic flora and fauna at each sile was

systematically sampled (with particular atten-

tion to hydroids) from the upper sublittoral

10 the seafloor at 50 m depth. Two additional

small epllections were also made—one in sea-

grass meadows in the more sheltered part of

Exsiern Cove, und another, at 65 m depth, 4

km to the south, between Pearson 7. and

Dorothee (Station F), Because of the rugged

nature anc exposure of the coastline to surf,

no collection of the intertidal fauna was made,

Collections

Holotype and paratype microslides, and

other microstides and material are lodged jn

the Nutional Museum of Victoria, Melbourne

(NMY), Paratype microslides are also lodged

in the South Australian Museum (SAM).

In most instances, the synonymy of Rulph

(1958, 196la.b, 1966) is adopted, and only

pertinent references to species in Australian

literature ure given. The status of several

species is reviewed to tesalye confusion in the

literature, and a number of rare and poorly

known species ate redescribed,

The site notation of Shepherd & Womersley

(1971) is followed, “R” denoting material col-

lected on the rough-water side of the island,

and “S” denoting the sheltcred side. Hydroids

collected in deep water at Stalion F are noted

separatcly. Depths at which cach species was

collected ure given. These depths will, how-

ever, represent only part of the total range of

each species. In most instances, the substrate

upon which each species was found is ulso

noted, As many hydroids ate hoth seasonal

and irregular in occurrence, it is likely that

collectiuns made at oiher parts of the island

HYDROIDS

or even at the same sites at other times, would

yield a slightly different faunal list.

The algal acology of these Pearson L. sites

is described by Shepherd & Womersley (L971),

who also list the algal species collected.

Ecology

Oceurrence af Hydroids

The collection yielded a large number of

species, in spite of the apparent paucity of the

hydroid fauna on Arst inspection of the locality.

Many of the species are crypuc forms growing

sparscly In small colonies among algae, where

only accessible with SCUBA. Even those

species (Selanderia fusca, Thecocarpus divari-

cates var. maccoyi, Aalicorearia longiroxtris,

H. prafifera) which are known to form con-

spicuous colonres in other localities, Were small

and attenuated, suggesting that conditions for

growth were not entirely favourable. This may

be due to the strong surge conditions around

the island preventing good grawth of the

colonies, or to the high light transmittance of

these waters, which appears to inhibit bydroid

growth (J. W. unpublished data).

The only athecate species, Tuhuleria larynx

and Selanderia fuseu, recorded from Pearson

I, were Found in relatively sheltered situations

on the rough-water site. Only one colony of

the former species, growing deep within a

euvern, was recorded, whereas the Jarter

spevics occurred as abundant small colonies

in sheltered situations among the holdfasts of

the brown kelp Ecklonia radiara.

The scarcity in rough ocean waters. of athe-

cate and other specics which liberate medusae

has ulready been noted at West, I. (Shepherd

& Watson 1970). Thua their absence from

Pearson I. is not surprising, considering the

exposure of the coastline to surf. Caripanu-

faria wustealis, a species likely to liberate

medusae, but whose reproductive strictures

ure still unknown, was however common on

the rough-water site, but only at a depth of

34-30 m, well below the zone of maximum

turbulence,

The collection from Station F, at 635 m

depth, yielded a markedly different fauna from

that of shallower water. The seafloor at this

station was tippleanarked sand, with tare

algae, a sparse epifauna of worm tubes, cal-

caréous hryozou, solitary acidians, and ald

shell. The dominant hydroids here were Syen-

plectoscyphus subdichotomus, S. fongithecus,

Syrtheciuin elegans £. subventricosumt and

Plamularia axsymmetrica The only species of

this group also fanging into shallower water

was S. slbdichoionius bit it Was uncommon,

P. asyrumetricg, the most abundant species in

the deeper water, has heen recorded only

three times previously, from adjacent waters of

the Great Australian Bight.

Reiaionship berween Hydroid anid Subsinate

Although little firm evidence of the associa-

fon between hydroids and substrate can be

gaincd on the hasis of ane series of collections,

a mumber of broad relationships aud possible

obligatory associutions are evident from the

Peurson [. material.

OF the total of &1 specres and 3 varieties, 27

urc exclusively epiphytic, 30 are non-cpiphytic,

und 18 are both epiphytic and epizoic, The

holdfast fauna, although strictly epiphytic, is

listed with epizoic, epilithic and "{ceegrowing”

species. (Table 3.)

A. Bpiphytie Hydroids (Table 2).

The two major families present, the Ser-

tulariidae and the Plumulariidue, are almost

equally divided between epiphytic and ¢pizoic

species. The Lineolariidae,. represented only by

Lineolaria spinulese, is epiphytic, Altogether,

47 species ate associated with red algac. mostly

on the rough-water sile, 27 species are associy-

ted with brown algue, and 3 species with green

algue, This is tn accord with findings at West

f. (Shepherd & Watson 1970) where red algae

were alsa the most heavily epiphytised group.

The most abuadant and widely distributed

species of algae had the greatest number of

hydroid epiphytes. Brown algae, particularly

Sargassum, although a substrate for fewer

hydroids, were often heavily epiphytsed by

luxuriant colonies of some common apecies

such as Amphishelia mininia var. pumiloides,

Plumularia epibracteolosa and = Sertularella

avrilia.

Several hydroids showed a hich degree of

selectivity and were ussociated with only ane

algal substrate (Table 2}, but as these species

Were not of common occurrence, it i uncer

tain whether an obligatory relationship actually

exists. However, there are two inslances of a

commonly occurring hydroid associated with

only one species of alga. Sertwaria acuta was

found only on the red alga Stenoeliadia aus-

tralix, whereas at West [. it wis abundantly

associated with the red alga Piacelecarpus

lahilfardier’. ‘The factors influencing the pref-

erence of §. acura for Stenocludia atustralfy, to

the exclusion of PRacerecarpus labitlardieri, at

Pearson I. are unknown.

The mast vonspicgtious assaciatinin Was thut

of Plamualarte epibructeoiosa with Use brown

ISG JEANETTE bE WALSON

alea Sargassum bracreolosuin, The fronds of

this alva were densely covered hy the hydroid,

in contrast to the stems which were exclusively

epiphytised by Amphishetia snininta vat.

puniloides. S. bracteolosunr was also recorded

at West |., but was epiphytised only by A,

aint and Campanularia ausivaliv.

Two other species, Lineolaria spinulose and

Plorindaria dastralis, were common epiphytes

tm the séagriss Posidonia australis, but were

not associated with algae. Colonies of both

hydroids were Frequently intergrown on, the

same blade of seagrass.

The growth habit of Phunuluria flexuosa

with a species ol the ved algal genus M yehedea

has not previously been reported, Usually

hydroids avoid algae with aw thallus of small

diameter (Nishihira 1967), The frond of

Muochodee sp., although somewhat Jurger than

the hydroid stolon, js nevertheless rather nar-

row. Vhe hydroid stolon passes length wise in-

letnally through the frond, giving off stems

to the outer surface at regular intervals.

Of particular interest is the gradational

epiphylism displayed by the Arniphisbetia

mininia-A, minuseule group, Bale (1884) dis-

tinguished var. pumtiloides from, var. intermedia

entirely upon the structures of the trophosome.

Hoth these varieties, and the closely related

species A. minusent, are abundant in the

present collection, und display a marked

gradational preference for certain groups of

ulgae—the robust var, pumilaides is found on

larec brown algac of the genus Sargassum (8.

varjans, §. verruculosion, S. bracteolosumy and

On Acrecerpia paniculaa; var. intermedia, a

small Lorm, is assuciated with the red algae

Rhodvinenia australis, Metamaytophera fabel-

lata, Levrencia élata, and Carpopeltis pipvllo-

Phord A, minuscula is both epiphytic and epi-

zuic and is associated with the red alga Lavrea-

cia elare, the brown alga Distromtium flabetle-

tum, a species of the green alga Caulerpa, as

well us being epizoie on Herdmania monnes

and Aalicornaria longirosiris,

B. Epizoic Hydroids

The Lafocidac, Syntheciidae and Halectidae

(with one exception Halecium sp. 1) are en-

tirely eépizoic. Generally, epizoic associations

are less well defined than epiphytic assacia-

tions, most of the species involved being found

on a wide variety of animal substrates, The

substrates upon which hydroids: were found

were, in order of abundance, other hydroids

(19 oceurpences), culcureous bryozou (15),

splines (4), the sulitary ascidian Herdnanig

mommies (l4), compound aseidians (3). und

muciliginous worm tubes. (2). Of the animal

Substrates, only A. moms and other hydroids

could be identified to species,

The two species of hydroids most commanly

enpizoitised by other hydroids are Thececarpas

divaricatus var. eystifera and Halicormmaria

longirastris, whose thick robust stems are sui

able for colonisation by the small stolonic.

species such as Syvaiplecroscyphus epizoicns,

Retieularia antarctica and R. gsnulare,

Herdmania rromus, one of the most ahun-

dint larger invertebrates at Pearson I,, grows

upon rock walls in open situations where there

is modetale water movement. The leathery

siphonal region of the ascidian is colonised by

small species of red algae, bryozoans and hy-

droids, the most commonly occurring hydroics

being Sertulerelle robusta, Sertularella sp. 1,

and Diphasia siebcar late.

C. Epilithic Uydroids

Epilithic colonies are usually conspicuous

plumose forms growing from small matted

routstovks wn rock surfaces in open situutions

where they can take: maximum advantage of

Water movement, This group, comprising

Thecocarpuy divaricaus val, eystifera, Malicey-

naria profifera, H. fonpiroyrris, and H. aurea,

all belong ta the Aglsopheniinae,

Closely allied in habit ta the true cpilithic

species are the lwo “freegrowing™ plumularian

species, Plumularia asymmetrica and Halop-

teris xtleda. Both wre large plumose colonies

growing from a small rootstock attached to

pebbles or shell fragments buried in the seu-

foor,

D. Ner-selective Hydroids

Species oceurring in both epizvic and epiphy-

lic habitats are often also associated with the

most ubunodyot animals ind plants, and are

thus amoung the most commonly occurring

hydroids, The most frequent of these multi-

preferential associations arc:

Hydeaied

Sertularella rohusra

Srebstrate

Ballia callipricha

Herdmania momus

Cavreneta eluta

Herdmania momus

Amenysla pinneri fides

Herdmania morass

Sertutwrelia sp 1,

Diphasia subcarinate

ee ee ee

Although many species (18) are both epi-

zoic and epiphytic, only 2 species, Thecocarpus

divericunsy and Halicarnaria longirostris are

epilithic as well. The largest of the 3 varieties

of FT. divuricetus, var. crstifera, is epilithic.

HYDROIDS 157

while of the 2 smallee varieties, var, 5rigesi is

pradational between epiphyde and epizoic, and

var, macceyi is epiphytic.

Distribution

All thecate families, with the exception of

the Campiunuliniidae, are represented in the

collections. Campanulariidae are represented

with 5 species, Sertulariidae with 31, Plumu-

lariidae with 31, Halecitdae with 5, Lafoeidae

with 4, Syntheciidie with 2, and Lincolanidac

with | species

With the exception of Thecocerpus divari-

cutus var. drives’ (previously recorded trom

New South Wales), ARericwaria antaretica

(Western Australia), and Zygophylax anti-

puhes (Torres: Strait), all other species newly

recorded from South Australia are known trom

Victorian waters, mostly from the intensive col-

lecting of Mulder & Trebileack (1909-1916)

along the central Victorian coustline, from Port

Phillip Heads to Torquay,

The new record for Australia, Syatheeiusa

dentigerum, has been reported only twice pre-

viously, once from the Indian Ocean, und once

from South Africa.

The genus Lyrocarpus, well known from the

Indo-Pacific region, ts recorded for the first

time (1, nuléer’) trom southern waters.

Only 14 of the 38 species listed by Black-

burn (1938) from the Sir Joseph Banks Ciroup

were in the Pearson I, collections. The two

groups of islands, however, are subject to dil-

ferent environmental conditions, the former

group of islands being situated in sheltered

water at the southern end of Spencer Gulf,

in contrast te the extreme exposure to rough

water of Pearson I. in the Great Australian

Bight. Comparison of the faunal lists of the

twa island groups shows thal the species com-

mon to both ure mostly specics epiphytic on

algae, and on the seagrass Pasidenia casusiralts.

Zoogeogruphy

Of the 83 specics and 3 varictics recorded

from Pearson |. 18 spectés are comnion to

New Zealand waters, 15 have a northern Aus-

tralian and western Indo-Pacific distribution,

10 specics occur jn South African waters, 6

are recorded from Japan, 2 from the Antarctic,

and 2 are cosmopolitan. Thirty-nine (49%) of

the species recorded (including the new

species) ate, us presently known, cndemic to

southern and south-eastern waters of Australia.

Blackburn (1942) estimated that 42%. of

the known hydroid Iouny of South Australia

Tanged into New South Wales, and 189% into

Western Australia, The present collection (with

1 variety common to N,S,W. and 2 species

common to W. Aust.) does not substantially

alter these estimates, The basis of comparison

between the 3 States is. however, poor, as both

the Jeep and shallow water hydroid fauna ot

South Australia as now better known from

SCUBA collections, whereas much of our

knowledge of the hydroid fauna of New South

Wales comes from deeper dredgings On the

continental shelf, and that of Western Australia

is from the reports of shallow water collections

between Albany and Shark Bay (Stechow

1924, 1925).

The 18 new records from the present colfec-

tion, combined with 18 from West T, (Shep-

herd & Watson 1970) brings the South Aus-

tralian bydroid fauna, based on Blackburn's

list, to 1 L9 species.

Thus, the total number of species common

to South Australia and Victoria is 81 (61%)

of the knewn South Australian fauna, This

fizure docs not differ greatly from Blackburn's

earlier estimate of 65%,

Based on Hodgson (1950), the fuuna com-

mon to both South Australia and Tasmania ts

69% of the South Australian fauna. Che

species common to Victoria and Tasmania

comprises 70% of the known Tasmanian

fauna. This distribution putlern lends further

support to the contention of Womersley & Ed-

monds (1958) that the Flindersian Province

embraces much of the Maugean, anil exterils

from the eastern Vicrorian coastline io at Irast

the central coastline of South Austritia.

Systematic Section

Order ATHECATA

Family TUBULARTIDAE

Tobutaria larynx Ellis & Solander, 1786, 31,

Bule, 1888: 748. Ralph, 1953: 68; 1966;

160.

Reeords: R, 24 m, on walls of cavern, shel-

tered from surge.

Material: One small cluster of stems to 2 em

high, Sven increasing gradually im diam, dis-

tally ts OS em. Perisare thick, smooth, wilh

groups of 3-8 annulalions; regrowth of broken

stems bepinning with a new series of annula-

tions. Hydranth 1.2 mm long, 1.0 mr wide,

but tentacles not fully extended. Proximal

whorl of tentacles a Jitthe longer tha clistul.

Gonophores small, spherical, sex tideterminate,

clustered between whorls of tentucies. Celoii—

tentocles white, gonophores pink

158 JEANETTE E. WATSON

TABLE 1

List of Species

Substrate notation; EZ = epizoic, Ep = epiphytic, El = epilithic, Fg = freegrowing, Hf = holdfast

fauna.

Symbols are given In order of abundance of colonies on substrate,

* denotes a new record for South Australia. .

The number preceding names of the species in the following list is the key to the species in Tables 2 and

ATHECATA

Family TUBULARITIDAE

1. *Tubylaria larynx Ellis & Solander, El.

Family SOLANDERIIDAE

2. Solanderia fusca (Gray). Hf,

THECATA

Family CAMPANULARIIDAE

3. Clytia (?) pearsonensis n.sp. Ez.

4. Campanularia ambiplica Mulder & Trebileock. Ep.

5. Campanularia australis Stechow. Ep, Ez.

6. *Campanuluria gaussica Stechow. Fz,

7. Campanularia sp. Ep.

Family LAFOEIDAE

8. *Reticuluria entarctica (Hartlaub), Ez.

9. Reticularia annulata n.sp. Ez.

10. Reticularia sp, Ez.

11. *Zygophylax anfipathes (Lamarck). Hf.

Family LINEOLARTIDAE

12. Linevlaria spinulosa Hincks. Ep.

Family WALECUDAE

13, *Ophiodissa australis (Bale). Ep.

14, Ophoidissa blackburni nsp. Ez.

1S. Phylactotheca armata Stechow. Ez.

16. Halecium delicalulum Coughtrey. Ez.

17. Halecium sp. 1. Ez.

18. Halecium sp. 2. Ep.

Family SYNTHECIIDAR

19, Synthecium elegans forma subventricosum Bale. Ez.

20. “Synthecium dentigerum Jarvis, Eu

Family SERTULARIIDAE

21. Thyroscyphus marginatus (Bale). Ep, Ez.

22. Parascyphus simplex (Lamouroux), Ez.

23, Diphasia subcarinata (Rusk). Ep, Ez.

24. Stereotheca elongata (Lamouroux), Ep.

25. Crateritheca acanthostoma (Bale), Ep, Ez.

26, *Crateritheca crenata (Bale). Ep.

27. Sulucia obliquanoda (Mulder & Trebilcock), Ep, Ez.

28. Sertularella robusta Coughtrey, Ep, Ez.

29. *Sertilarella simplex (Hutton). Ez.

30. Sertularella annulaventricosa Mulder & Trebileock Ep, Ez.

31. Sertulareila avrilia n.sp- Ep.

32. Sertularella sp. 1. Ez, Ep,

33. Sertularella sp. 2. ?

34. *Symplectoxcyphus longithecus (Bale). ?

35. Symplectoscyphus subdichotomus (Kirchenpauer). Ez.

36. Symplectoscyphus neglectus (Thompson), Ep.

37, Symplectoscyphus indivisus (Bale). Ep.

38, Symplectoscyphus pygmaeus ?(Bale), Ez.

39. Symplectuscyphus macrothecus (Bale), Ep.

40. Symplectoscyphus rostratus n.sp. Ep, Ez.

41. Symplectoscyphus epizoicus n.sp. Ez.

42. Sertularia macrocarpa Bale. Hf.

43, Sertularia iinguicilata Busk, Ez, Hf.

44, *Sertularia bicuspidata Lamarck. Ep.

45, Sertularia maccallumi Bartlett, Ep.

46, Sertularia acuta Stechow, Ep.

47, Amphishetia maplestonei (Bale). Hf.

48. Amphisbetia pulchella (Thompson). Ep, Ez.

49, Amphisbetia elyeni n.sp, Fz, Ep,

HYDROINS 159

50. Amplishetia minima var. pumiloides Bale, Ep,

St. Amphixhetia minima var. intermedia Bale. Ep. Ez.

32. Amphishetia minuscula (Bale). Ep, Ez.

Family PLUMULARTITDAK

33. Pyenotheea producta (Bale). Ep.

54. *Amtennella tubulosa (Bale). Ep

“Antennella campuniliformis (Mulder & Trebilcock). Ep.

56. *Antennella secundaria s.sp, dubiafermis (Mulder & Trebilcack ), Ep,

37. Halopteris suleata (Lamarck). Fe.

38, Halopteris campanila var. campanula (Busk). El,

59. Halapteris biuski (Bale), Fz.

60. Halopteriy oppasita (Mulder & Trebileack). Ep.

61. *Gaitva bale (Bartlett). Ep.

62. Gattya uglaopheniaformis (Mulder & Trebilcock). Ez, Ep.

63. Gaftya trebileovki nusp. Ep.

64. Plumularia procumbens Spencer. Fl.

65. Plumularia asymmetrica Bale, Fg.

66. Plumutaria flecnosa Bale. Ep.

67. Plumularia spinnlosa Bale, Ep. Ez.

68. *Plumularia goldsteini Bale. Ep.

69. Plumularia obliqua (Johnston). Ep.

70, Plumularia australis Kirchenpaver. Ep.

71, Plumutaria epibractealosa n.sp, Ep.

72. Plumularia meretricia asp. Ez.

73. Plurmitlaria togata n.sp. Ep.

74, Plimularia australiensis n.sp. Ez,

75, Aglaophenia plumosa Bale. Fz, Ep.

76. Thecocarpus divaricatiis yar. maccayi Bale, Fp.

77. *Thecocarpus divaricatus var. brigest Bale. Ep, Ez.

78. Theeocarpus divaricutys var. cystifera Bale. Fl.

79. *Lyvtocarpus mulderi (Rartlett). ?

80. Malicarnopsis elegans (Lamarck). E}.

81. Halicornaria longirastris (Kirchenpauer). FJ, Ez, Ep.

82. *Halicornaria prolifera Bale. El.

83. Halivernaria aurea np. EL

Remarks; This cosmopolitan species was douht-

fully recorded for the first time from Austra-

lian waters by Ralph (1966) who reported a

few infertile stems from Port Phillip Bay, Vic,

This is the second tecord of the species in Aus-

tralia, and a new record for S. Aust.

Solanderia fuseq (Gray, 1868). Watson é& Uti-

nomi, 1971; 19, pl. 8.

Ceratella fusca (Gray), Spencer, 18915 &-

Records: R, 14-33 m, among holdfasts of

brown algac.

Material: Four very small infertile colonies

broken off from the rootstock, the largest

colony 5S mm high and 20 mm _ wide.

Colonics compact. branching closely in one

plane from a thick main stem, Srem of largest

colony 3 mm wide at base, stem and branches

flattened in plane of growth. Aydrophores are

Open shelf-like structures, prominent on

younger branches, edged with 10-15: bluntly

pointed terminal spines connected by a thick.

shallowly scalloped chitinous web. Trabecilate

meshwork of branches close and solid, with

square to circular openings, Spires similar to

those edging hydrophore developed at points of

intersection of meshwork on older branches.

iTvdranuths poorly preserved. Colour—stems

dark brown, shading to ight brown on grow-

ing tips.

Remarks: The colonies of §. fitsce from Pear-

son J., although dwarfed and infertile, are

mature, occurring among algae on horizontal

rack faces. This. is in contrast to the known

habitat of larger specimens from Victorian

waters, which seem to favour vertical walls

and the interior of caverns (J.W., unpub-

lished). Bale (1888, p. 749) mentions that his

small colonies from Sydney were from “Lamin-

aria roots” (probably Ecklonia radiata hold-

fasts). Watson & Utinomi (1971). reported that

the spinous trabeculae were not present in

material examined by them from the Great

Australian Bight, vet the Pearson J. specimens

show these spines clearly. Unknown environ-

mental and geographical factors may thus in-

fluence structural variations within the species.

Order THECATA

Family CAMPANULARIIDAE

Clytia (’) pearsonensis n.sp_

FIG. 2

160

JEANETTE E. WATSON

TABLE 2

Fpiphyic Hydroiils

The numbers tefer to the species as given in the species list.

VC = very common, C = common, R = rare,

Aleal Substrate Hydroid

CHLOROPHYTA

Canlerpa brownii (C.Ag.) Endlicher. 63(R)

Cailerpa staplicinsenle (Turner) J. Agardh. T7(R)

Caulerpa sp. 52(VC)

PHAEQPHYTA

Disrominm flabellaium Womersley. §2(VC), 53(R), 56(R)

Distramium sp. 37(C)

Zonaria spiralis J. Agardh. Ta(VOY

Sevtotlalia darvcarpea (Turn.) Greville. 24(VC)

Acrocarpia paniculala (Turn) Areschoug. 24(VC), 39(R), S0(VC), 76(VC)

Cystephora brownii (Turn, ) J, Agardh, 5(C)

Sargassum verruculosum (Mert-) I Agardh. 31(C), 40(C). 60(R)

Sargassum hractéolesum J. Agardh. S0(VC),7I(VC)

Sargassum spinuligerum Sonder,

Sargassum Varians Sonder.

Sargassum 8D,

RHODOPHYTA |

Delisea pulehra (Grev.) Montagne.

Preracladia lucida (R.Br.) J. Agardh.

Rhodopeltis anstealis Harvey.

Metazoniolithon chargides (Lamx.) W. v. Bosse.

Metamasiophara flabellata (Sond.) Setchell,

Carpopeltis phyllophara (A. & A.) Schmitz.

Callopha lis caccinea Harvey.

Plocamium aneastune (J, Agardh) Hooker & Harvey.

Hacamium cartilagineum (L.) Dixon.

Phacelocarpus labillardieri (Mert.) J. Agardh,

Stvenoclacdia australis (Sond.) Silva.

Alvehodea sp,

Rhoadymenia anusiratis Sonder.

Ballia callitricha (C.Ag,) Kuetzing.

Prerosiphonia?

Anunsia pinnatifida Harvey.

Laurencia clata (C.Ag.) Harvey.

Inidentified red algac.

ANGIOSPERMAE

Pasidonia australis Hook. f.

37(C), 50(VC), 60(R)

sa.VC), 55(R)

21(R), 30(C), 36(VC), I7(C), S4ER), 69(R)

48(R)

5(C), 36(VC), 45(VC). 48(R), 55(CY

61(C)

44(R)

27(VC), 36(VC), 73°VC)

44(R), SICVC), 61(C), 69(R), T6(VCO)

45(VC). 75(R)

62(R)

67(C)

7T6(VC)

24(VC)

24(VC), 46(VC)

66(R)

SI(VC), 56(C)

28(C)

61(C)

23(VC)

32(VC), Si¢VC), S52°VC), SS(C),

67(C)

4(R), 70K), 25(R). 27 (VE), 30(€). 36(VC).

40(R), 49(C), 53(R), T7(R), STC VO)

12(VC), TOCVE)

37(C),

Type Material and Records; Holotype,

NMYV G1914, microslide—R, 22 m, on stem

of Thececarpus divaricatis var. cystifere;

paratype, G1915, microslide—R, 34 m, on

bryozoa.

Description from holotype and paratype: Pedi-

cels long, of variable diametcr. irregularly

wrinkled or smooth (holotype shows indistiact

distal annulations), arising from a creeping

stolon. Hydratheede large, cylindrical. walls

smooth, perisarc very thin and delicate, mar-

vin entire. everted into a thin lip. Thecal wall

slightly thickened proximally, hydrotheca with-

out floor, tapering inta pedicel, a trace of a

very thin diaphragm near base. Hvdranth too

poorly preserved for diagnosis, Ganotheca ab-

sent,

Remarks: Only 2 undamaged hydrothecae were

found im the entire collection, although othet's,

badly damaged, were noted. It is possible that

the species has previously been overlooked

hecause of the extremely delicate nature of the

perisare, which collapses immediately on re-

moval from water.

C. pearsonensiy ts closely related ta Lao-

medea michael-sarsi Léloup, 1935, reported

from only two localities—the West Indies, and

the west coast of North Africa. The hydro-

theca of L. michael-sarsi are, however,

shorter and less than half the diameter of C.

pearsonensis. (Measurements ate given for

camparison),

Following Millard (1959, p. 248), the

species may be referable to cither Campatu-

HYDROIDS 161

TABLE 3

Epizoic, Epilithic, Freegrowing and Holdfast Associations.

Substrate

Wydroid

Epizoic Species

Ascidian— .

Herdmania momus (Savigny)

Compeund ascidians

Sponge

Calcareous bryozoa

Worm tubes

Other Hydroids—

Synthecium sp.

Thyroscyphus marginatus (Bale),

Sertilaria unguicilata Busk.

Symplectoscyphus subdichotomus (Kirchenpauer ).

Halopteris campanila var. campanula (Busk),

Plurnularia proeuntbens Spencer.

Thececarpus. divaricatus var. cystifera Bale.

Halicornaria longirastris (Kirchenpauer).

Epilithic Species

Freeerowing Species

Tloldfast Species

Cc. pearsonensis 1.. anichael-sarsi

Yi Ww.

halo nara * A

Dinension, mm tyre type Africa Tndies

Stem length 1.80 1.32 = 1.00-1,50

dium. 007 017 _ O.1-0.15

Hydrotheca—

Width af margin 0.58 O68 0.25 0.25-0,30

0.69 O65 0.40 0,50

depth to diaphrasta O78

laria or Clytia. The barely discernible dia-

phragm and very delicate thecal wall suggest it

may belong to the latter genus, but its system-

atic position is indeterminate until fertile

material is found.

Campanularia ambiplica Mulder & Trebilcock,

1914: 11, figs, 2-4, Shepherd & Watson,

1970: 140.

Paracalix ambiplica (M. & T.). Stechow, 1925:

209, fig. EB.

Recards: S, 5—14 m, on red algae

Material: Three infertile stems. Stems short,

spirally annulated. Hydrothecae long, narrow,

walls parallel, a very strong S-shaped fold

about halfway along thecal wall. Margin with

6 teeth, cach with several reduplications.

Remarks: Type material of C. ambiplica in the

collection of the NMV shows more campanu-

late hydrothecue with blunter and less deeply

excavated marginal teeth than the Pearson I.

14(C), 16(C), 19(R), 20(R), 21(R), 22(R),

23(VC), 2B(VC), 29(R). 32°VE). 3R(C);

43(R), 49(C). 59(R)

15(R), 38(C), 75(R)

5(C}, 9(R). 13(R), 14(C), 15(R), 25¢R),

27(C), 28(VC), 38(C), 49°VC), 56(C),

§9(R), 74(C), 72(R)

3(R), 6(R), 10(R). 14(G), 27(C), 2B(VCd,

29(R}, 30(C), 32(VC), 35(R), 38(C),

40(R). 59(R), 75(R). BLEVC)

19(R), 59(R)

16(C)

67(C)

20(R), 56(C)

TT(RY

32(C)

16(C), 62(C)

3(R), B(VC), 19(R), 22(R), 29(R), 38(C),

4i(C)

8(VC), 17(R), 41(C), 520VC)

1(R). 58(R), 64(C), 7R(C), BOR), BICVC).

82(R), 83(C)

S7(C), 65 (VC)

2(@), 11(R), 42(C), 4300), 47(C)

specimens. Stechow's figures of specimens from

Champion Bay, W. Aust. aré intermediate in

length between the two. Meussurements are

given for comparison.

Victoria

Diwensions, nm Peai3on L. Champion Bay (M. & T)

Stem diam. 0.06 0,06 0.06

Hydrotkeca—

fongth 1,52 0.42 0.34

width DAT O18 0.17

Campanularia australis Stechow, 1924: 61.

Shepherd & Watson, 1970: 140.

Orthopytis australis (Stechaw). Hirohito, 1969:

10, fig. 9.

Records: R, 34m, on the algae Pteracladia

lucie, Cysiophora brownii, and sponge.

Material: Stems variable, to 3 mm tong, longer

slems smooth, short stems annulated, Aydro-

thecae compressed, with a wide submarginal

flange and 9-10 blunily pointed teeth, in one

instance showing reduplication. Aydranih with

16—20. tentacles, Colonies fertile.

Remarks: Although widely distributed at all

depths and on a variety of substrates, the

colonies were. not luxuriant.

162

Caumpantilings

1924; 62,

guussica Stechow, 1923: 102;

FIG, 3

Record: S24 m, on calewrcous bryazoa-

Miverial: Three infertile stems, Sremes to 4 rom

long, shewing jomts where breaks have fe-

generiuled, A spherule between stem and bydro-

theea. Hydretheeae large, campanulate, 1.26-

1,32 mm deep, expanding evenly from a nar-

row base to margin, an annular diaphragm in

thecal cavity. Margin variable in diam., 0.78—

1.2 mm, with 12 deep tongue-shaped teeth

0.015-0.618 mm wide at base, 0.013-0.015

mm long, the sinus hetween of same shupe and

size as tooth. Aydranth with approx. 16 ten-

tacles surrounding a thick annular hypostome,

similar to that of Eiclenedr/um,

Remarks; The Pearson J, specimens are among

the largest specimens of Campanularia

recorded from Ausiralian waters, the only other

specimen of comparable size being “Campanu-

lavia tinera var." of Mulder & Trebileock

(19149). from Brey Creek, Vic, (see dis-

cussion below), This is a new record for S.

Aust.

Remarks on whe states of Co tinela Hineky,

1867, C, giussica, and C. australis,

Stechow (1925, p, 206) placed Mulder &

Trebileock’s vars. ‘“‘a", “b", “co” snd “a” of

C. tineta in tentative synonymy with C. peur

sica, However, the dimensions of the hydrothe-

coe calculated from Mulder & Trebilcock's

figures are somewhat greater than Lhose given

by Stechow for his specimens. Moreover, his

figure does net show the annular diaphragm

figured by Mulder & Trebilcock, a feature alo

presentin the Pearson T. specimens.

Earlier, Stechow (1924) stated that the

gonosame of CG. gaussica was unknown, yet in-

cluded in his synonymy (1923, p. 102) a

questionuble reference to the C. tincra of Bale

(1884, p. 57) from Portland, Victoria, for

which the ponutheca was figured. He later te-

ferred Bale’s species ta C, langitheca without

explanation. The Portland specimen ih the col-

lection of the NMV is undouhtedly C, australis,

nul C. gansefew.

T cjinnot agree with Rees & Thursficld

(1965, p. 94) who reterted ©. gansyica to the

synonymy of G. dincta, The latter is a very

smal) and distinctive species; although they

stated they had examined the type material of

C. iieta, they failed to ote the very con-

siderable difference in size between the two.

The definition of the Four species, C) zincrer,

C, ausrralis, C. gatssiea and C, africatia, from

IEANETTE FE. WATSON

Austratian waters rs thus somewhat confused,

Although €, tiara and C. australis are very

similar, with bilaterally symmetries! hydro-

thecae, C’, ansrralis ts considerably the larger of

the two. ©. dugfralis shows a wide choice of

substrite, being bolh epizoic and epiphytic,

whereas C. tinete appeurs to be most Frequently

assochited with the seagrass Amphibolls antarc-

tica LW, unpublished),

Wirohity (1969, p. 10) transferred C. any-

tralis to Orthapyxts on the basis of the bilateral

symmetry of the hydrotheca, but the true

gencric status of C. australiy will remain inde-

terminate until the gonosome. is found.

C. africana is a distinct species, and has

been redescribed by Millard (1966, p, 474),

The hydrotheca is of medium size and the

gonosome is known. This species. has been re-

corded from Queensland (Pennycuick 1959, pp.

169), from “rock poals and weed”,

Uniil the collection of fertile material estab-

lishes the validity of C, waswralis and C, gays-

vica, those forms from Australian waters with

very large campanulaie hydrothecae and 10-14

tongne-shaped teeth are recognized as (". guus-

sie, those with large parallel-walled hydro-

theeae and bilateral symmetry are recognized

as C. austrafis, and those similar to C. atastralis

but much smaller in size, as C, tinere. In the

gase of C_ gaitssica, it is possible that more than

One species may actually be involved,

Campanularia sp-

FIG. 4

Records; S, 17-20 m. on red atgac.

Mfarerial: Three infertile stems. Srems 0.51—

1,72 mm long, spirally annulated, annulations

sometimes indistinct, maximum width of stem,

04 mm. Aydrothecae campanulate, length

0.39 mm, widest about one third distance

up from base, this point belng marked by a

crumpled fold encircling thecal wall. Base of

hydrotheea flat, with o slight concavity, a

socket and xpherule between hydrotheca and

stem. Margin 0.22 mm in diam, with & hroad

fongue-shoped teeth 0.025 mm high; width be-

tween tecth, 0.06 mm.

Remarks; The hydrotheeac are very delicate,

Although the hydrolthecae are somewhat col-

lapsed in mounting, the fold around the proxi-

mal region of the thecgl wall is clear in all

specimens,

The specimens are undoubledly referable to

the C. ambiplica-C. pulechratheca group en-

demic ta southern Australian waters, most

resembling the latter species, However, ©,

IL¥YDROIDS 163

Reticularia annulgfa nsp, Fig, 5—Group of three hydrothecac Fig. 6,—Distal chd of

Fig. 2 Clytia (?) pearsonensis n.sp. Hydrotheca, from holotype.

Fig. 3- Campanuluria ganssica Stechow. Hydrotheca; stem with regenerated pedicel,

Fig. 4, Campanularia sp. Hydrotheca.

Figs. 5,

hydrotheca, enlarged. Drawn from holotype.

Figs. 7

.8. Reticularia sp. Fig. 7.—Part of colony, showing growth habit on bryozoan colony. Fig.

8 —Hydrotheca, enlarged, showing reyenerated distal end.

pulchratheca has 14 sharply pointed teeth, the

intrathecal fold is in the distal region, and

does not encircle the thecal wall as in the

present material. This may be a new species,

but the material is inadequate for determina-

tion.

Family LAFOEIDAE

Reticularia antarctica (Hartlaub, 1904). Tot-

ton, 1930: 160, fly. 17, Briggs, 1938: 26.

Eafoas antarcti¢a Hartlanb, 1904; 11, pl. 2, fig.

Filellum

1925: 214.

Recards: R, 18-33 m, on stem of Thecoeer-

pus divaricatus var. cystiferu. S. 14 m, on

stem of Halicarnaria longirostris.

antarcticum {Hlartlauh). Stechow,

Materia/: Luxuriant infertile colonies, Hydro-

thecae delicate, of variable length, arising at

various ungles from hydrorhiza so thickly that

it is difficult to determine the length of the

adnate part, but it is usually not more than

one quarter of the total length of the hydro-

theea. Margin slightly everted, often with 2-3

teduplications; occasionally an earlier redupli-

cation about halfway along hydrotheca coin-

cides with a slight flexure of the thecal wall.

Length of free part of hydrotheca, including

reduplications, 1.0-1,18 mm; diam. at margin,

0.21 mm.

Remurks: Mt is very difficult to distinguish be-

tween R. antarctica and R, serpens in the

absence of coppiniac, and as the diameter of

the (hecal margin is greater than those measure-

ments given by Stechow (1925, p. 214) for R,

serpens (after Millard 1958, p. 175), the Peur-

son |, spccimens are referred to R. antarctica,

This is the first record of R. antaretica from

S. Aust. waters. (Other locality—W, Aust.)

Reticolatia annulata n.sp,

FIGS. 5. 6

Type Material una Records: Holotype NMV

G1922, microslide: G2091, preserved

Malerial, remuinder of holotype colony—sS,

L7.m, on a small calcareous bryozoa.

Description from holotype: Hydrothecae bong,

tubular, inereasing slightly in diameter disttlly,

adnate for a sroall part of length, free pari

0.15-0.18 mm, curving out from hydrorhiza,

Hydrorecae ringed throughout eatire fength

with closely und evenly spaced annular ribs,

average distance between ribs U-US mm, each

rib with shatply everted rim; unnulations on

adgauline wall not as shatply defined us those

on free wall, Margin circulur, entire, same

diam. as hydrotheca, 0.19-0.26 mm, occtasion-

ally sinucusly curved, with everted tim. Gono-

theca wbsent,

Remarks; R. annntata is closely related to both

R. antarctica {Wartlaub, 1904) and R. serpens

(Hassall, 1848) jn shape and dimensions of the

hydrotheca, but it is easily distinguished from

these species by the close thecyl rings, FR,

serrata (Clarke, 1879) Is annulated, but the

wnnulations are confined to the adnale part of

the hydrotheca, and it is 4 much smaller

species.

The rings in R, canulatea are o£ uniform size,

and the distance between them varies. litte

along the entire length of the hydrotheca. They

have developed by continuous apical reduplica-

tion during growth of the hydrotheca, the

flange of each rth being a relict margin.

Reticufaria sp.

FIGS. 7, 8

Recerd: R, [S m, colony investing stalk of

calcareous bryozona,

Materiel; One infertile cdlony. Hydrethecue

arising in groups, or singly at irregular inter-

vals, Hydrothecac from the outer hydrorhizal

tubes adnate for approximately half their

length, free part standing, out almost perpen-

dicular to hydrorhiza. Length of free part 0.45—

0.66 mm, only the orifice of those hydrothecue

more deeply embedded in the stolonic camplex

visible. Hydrothecac tubular, 0.2 mm in diam,,

IEANETTE,

E. WATSON

many with Z—3 regeneractions after breakage.

some with marginal reduplication. Cole.e—

brown.

Remarks: The general appearance of the

hydrothecae and the diameter of the margin

ure very similar to R. antarctica from Pearson

L., but the hydrothecae of the present specimens

are much shorter; the thick woody fascicled

hydrorhizal tubes further distinguish the

present material.

The twiggy appearance of the colony, iin-

parted by the shape of the host, strongly sug-

gesis the growth habit of Cryprolaria, but with-

out the regularity of arrangement of the hydro-

thecne of that genus.

This may prove to be a new species

Zygophylax antipathes (Lamarck, 1816). Rees

& Thursfield, 1965: 76.

Sermilaria antipauthes Lamarck, 1Bl6: 11S,

Campandlaria rufa Bale, 1884: 54, pl. 1, fig. 1.

Efesoneiia antipaties (Lamarck), Ritchie, 1910;

Zygophylax rufa Bole, 1914¢: 90,

FIG, 9

Records: R. 18-45 m, among holdfasts of

hrown algue on vertical walls and on the

seafloor.

Muarevieal: Three infertile colonies, the largest

12 em high, growing from a small rootstock,

Stew woody, very brittle, main stem fascicled

(2 mm thick in largest colony) the fasciculu-

tions decreasing distally along the branches.

Branches given off randomly around main

stem. some of younger branches mono-

siphonic, /lydrothecae alternate, 0,32-0,34

may deep (margin to diaphragm) arising from

an upoaphysis at 45° to stem, frequently a short

segment (a broken und regenerated pedicel of

an earlier hydrotheca). between Nycdrothecul

pedicel and apophysis, Adcauline thecal wall

convex, 0.30-0.37 mm long, usually smooth,

sometimes. a little undulated; abcauline wall

straight or slightly concave, 0,30+0,36 mm

long. Margin usually with a distinctly everted

rim 0.17 movin diam., occasionally with | re-

duplication, Diaphragm near base of hydro-

theca transverse, occasionally oblique. Nemiato-

thecae pare, only 2 seen in mounted specimens,

one given off from a hydrothecal apophysis,

the ather from a polysiphonic tube of the stem.

Colour—aeep reddish brown,

Remarks; The branches are overgrown with

algae and conipound ascidian,

Bile (1914¢) maintained the distinction

between Z. rufa and 2, antipathes on the fal-

lowing cntenas

HYDROIDS

(i) the smaller colonies of Z. rufa, the lack

of rigidity of the branches, and,

Hid L. antipathes, following Billard, shows

no distal narrowing of the hydrotheca,

nor an everted margin.

Examination of a series of microslides of Z,

ea in the collection of the NMV, show. Bule’s

material to have come from either a broken

branch, or the distal end of a very young

colony, and there ate few hydrothecae which

are not hoticably narrowed distally; some also

lack an everted margin. One branch of the

Pearson L material bas a series of hydrothecse

with almast straight walls, no eversion of the

margin, und a rather more delicate perisarc

than usual,

Regenerated hydrothecal pedicels with an

additional segment are common in the older

regions of the stems, but are net present in the

Younger branches. They are a character de-

veloped with aging of the stem, and are thus

not specifically diagnostic.

I have compared microslides of Ritchie's

“Thetis” material of Lictorelle artipathes with

Z. rufa of Bale, and find them to be identical

in all respects, except that the perisare of Z.

rufa is much more delicate than that of the

“Thetis” specimens.

Ritchie did not comment on the presence of

nematothecae (similur to those on the Pearson

I. specimens) visible in his slides. These were

apparently noted by Rees & Thursfield (1965)

who transferred the species 10 Zygopliylex

without comment.

Since the present material has features which

clearly bridge the gap between Z. rufa and Z.

antpathes, the Wwo are considered synonymous,

This is the first record of Z. aniipathes in

S. Aust. waters. (Other localities—Torres

Strait, and off Port Jackson, N.S.W.)

Family LINEOLARIIDAE

Lingokwia spinulosa Hincks, 1861: 280, pl. 8,

Shepherd & Watson, 1970: 140.

Record: S, 15 m, on the seagrass Posidenia

ruasrrialts,

Material; Numerous infertile colonies over-

Tunning the blades of the seagrass.

Remarks: L, spintlose was not found on any

other substrate at Pearson L,

Family HALECUDAR

Ophiodissa austratis (Bale, 1919).

ph renles avairaliy Bale, 1919- 396, pl. 16, fig.

Record: R, 19 mi, On black sponge.

165

Material: One colony of several infertile stems

growing from a matted hydrorhiza on the sur-

fuce of the sponge, Sremx to 2 cm long, fas-

cicled, itregularly branched, with 2-3 supple-

mentary tubes extending two thirds the distonce

up stem. Aydraphore with a few reduplica-

tions. WNematothecae rare. Crleour—light

greenish, with black patches scattered through-

out hydrocaulus. (Under the microscope these

pitches are black granules concentrated on the

hydranth and in the coenosyre.)

Remarks: The status of Ophiodissa haa been

briefly discussed by Watson (1969, p, LIN),

Bale (1919) described, but did noe figure the

gonophore of O. australis, Ralph (1953, p,

342) way. uncertain whether @. australis is a

synonym of Hydrodendroy — cacinifarmis

(Ritchie, 1907) but kept the two apecies

separate because “the hydrothecae of 4, aus-

tralix Bule are shallower, measured fromm the

margin to puncta line, than those of H. cuvini-

formis, und the goncthecae of the latter are

unknown". Millard (1966b, p. 490) described

the gonophore of H, caciniformis fiom material

from the Vema Seamount. off the west coast

of South Africa.

There are two microslides of O. australis in

the Bale collection In NMV, one trom Green

Point, N.S.W,, and the other from Port Phillip

Heads. Vic. The latter specimen is 4 lightly

fascicled stem 2 cm long, with u group of 10

male gonophores growing {rom the hydrohiza,

and is undoubtedly the slide fram which Bale

described the gonotheca of the species.

The gonothecae aye smooth or very slightly

wnnulated, with curved or straight pedicels, and

several have a slight constriction just below ihe

truncated distal end, The gonopheres are

nearly mature, the blastostyle almest filling the

gonothecal cavity, aod above the blasroscyle

there ts a ring of black granules,

The gonothecae and gonophores of Bale’s

material are similar to those of A, caciniformis

figured hy Millard, but the ponotheca of O..

australis is much longer and more than twice

the width of those of JT. caciniforinis, Further-

more, the hydraphote of HW. cacinifprmiy (trom

Millard’s figure) is both wider and deeper than

that of Q. ausiralixs from Green Point, It seems

that the two species, while very similar, are

distinct,

Comparison of measurements (see helaw)

of HH, caciniformis from New Zealand with

Bale's Q. australfe shows that the New Zea-

land maternal Falls near the dimensional range

of OO. aeuwealls, and may well be this species.

Lob JEASETTE, E, WATSON

The finding of fertile material in New Zealand

waters will settle this. point.

O. australis

Dimensions, mm H. caciniforialy

Pearson Grein N: 8.

I, Pi. Fealand = Africa

Uycirophore— .

diam, 1 Paneta dine 0.14 0.15 0,12 0.20

depth, margin to

puacta ne 0.025 O05 0.44-4,06 0.10

Gonotheca

length t.441.50 — 6 90-1,90

width at mporpyre — 0.94-1.00 —_ 0.40

The specimens from Pearson I. are identical

im every respect with Bale’s 0. australis. This

is the first record of O. awsrralis from §. Aust.

Ophiodissa blackburni a.sp.

FIGS, 10-12

Type Material and Records: Hoaletype.

NMV G1927, microslide; G2092, preserved

material, remuinder of holotype colony—-S,

27 m, on Herdinuiia monus; Paratypes

GI928, G1929, microslides; G2093, pre-

served material, reémuinder of paralype

colony—S, 24-27 m, on bryozoa and

sponge.

Description from holatype ard paratypes:

Hydrorhiza a winding tubular stolon 0,11-0,13

mm in diam,, thick and strongly corrugated

throughout entire length, becoming erect at

intervals 10 form monosiphonic stems. to 12

mm high, Uydrephores given off irregularly,

either directly from the siolon or from stem,

Pediccl of hydrophores of variable length,

0.19-0,27 mm, beginning with an annular con-

striction 0,07-0,10 mm in diam., followed by

1-2 annulations, then expanding evenly to: mar-

gin, Perisarc thin. Secondary and tertinr'y

hydrophores common, branching outwards just

below the diaphragm ot primary (or secon-

dary) hydrophore, becoming ascending at an-

nular constriction. Hydrophores: redupliculed

up to 4 times; reduplications of variable length,

given off successively from the diaphragm of

preceding hydrophore, Diaphragm 0.13-0.17

mim in diam., moderately deep, 0.04 mm from

margin (best seen in preserved material). Afur-

vin flaring, with strongly everted lip, diam,

0.22-0.24 mm. Neutothecae sparse low tubu-

lar orifices 0.03 mm high, and 0,05 mm in

diam, at base, situated on hydrorhiza or stem,

opposite, or nearly opposite hydrothecal pedi-

ecl. Aydranth large, extensile, with approx. 30

stubby tentacles. Co/lawr—yellow, Gonetheca—

absent.

Remarks; The presence of nematothecae places

the present material in Ophiodissa (Watson

1969, p. 111). Although in. some instances the

hematothecae may be mistaken for the broken

hase Of a hydrothecul pedicel, their position

opposite the pedicel, and their smaller size

usually serves to distinguish them.

O. blackburni shows some resemblance to O.

carrugata Praser, 1936, However, neither

branching nor reduplication of the margin is

mentioned or fizured by Fraser, and the ten-

ticular orguns of O. currugata are described as

being relatively large and flaring slightly at the

marfgin (Fraser 1936, p, 113).

Blackburn (1938, p, 322) described a frag-

mentary Haleciunt sp. Crom the Jittoral zone

of Reeyesby L in the Sir Joscph Banks Group.

S. Aust., remarking that the material, too ob-

scured by forcign matter for diagnosis, Was

probably a new species, similar to A. corra-

garuen Nutting, 1912. Although Hlackburn's

specimens are not available for comparison, it

is certain that his milerial aimel the present

specimens are the same species.

Phylactotheca armata Stechow, 1924: 54:

1925; 204, fiz. C. Blackhurn, (942° LOA,

Ophtiodiata Jrogitts Blackburn, 1937a! 365, fig.

Records; R, 33 m, on sponge and ascidian,

Maserial: A few infertile stems to | em high.

Renuirks; The Pearson I. material conforms to

the description of the species given by Stechow

and Blackburn.

There are no secondary hydrophores, nor

any nematothecac developed in the present

material, Blackburn's specimens from Balnar-

ring. Vie., similarly showed no sign of nemu-

iothecac, Hence their presence or absence cam

not be taken as a good diagnostic character

lor Lhe aenus,

Halecium delicatulum Coughtrey, 1876: 299,

Ralph, 1958: 334, figs. 11, 12. (syno-

nymy),

Records: R, 21-45 m, on Plamularia pro-

cemberns and Syntheciunt sp.; 8, 24 m, on

Herdmania momus, and brvozoa,

Material: Miny small infertile stems to 2 om

high. Sresns irregularly and sparsely branched,

a few are lightly fascicled, with an extra poly-

siphonic tube running up the proximal part of

the stem.

Renuirkay Oye of the mest abundant epizoic

species tm the collection,

HYDROIDS UG7

Halecium sp. 1.

FIG, 13

Record: R, 30 m, an lower stem of Halj-

cernarie fongirostris,

Moreelul’ A single infertile stem L2 mm high.

Stem unfascicled, irregularly branched; stem

and branch intemodes of vanable length, up

to 0.22 mm, and 6,04 mm in diam., annulated

proximally, but otherwise fairly amooth-

Branches given off from distal end of inter-

nodes on lower part of stem, Pedicel of pri-

mary hydrephore of yariable length, proximal

node transverse, follawed by 1-2 antulations,

the remainder smooth, expanding evenly to

diaphragm. Aydrophere small, shallow, with

circular margin, 0.08-0.12.mm in diam., and

strongly everted tim; up to 3 reduplications

given off successively from mouth of preceding

hydrophore. Diaphragm present, depth from

margin to diaphragm, 0.02-0.03 mm. Secearn-

dary and tertiary branches comman, arising

from distal end of pedicel of primary (or

secondary) hydrophore,

Remarks: This very small form resembles H.

tenelliom Hineks, 184) in size and delicacy of

the trophasome, btit the dimensions are ever

smalfer than those given by Millard (1957, p.

193) and Rilph (1958, p, 340) for this

species.

in the present material, only the first inter-

node can be described as a true stem, the

branching being truly arborescent, all sub-

sequent internodes being secondary branches

given off the pedicels of the primary hydro-

phores. The presence or absence of punctae

cannot be ascertained because of foreign mat-

ter, However, the Bale collection in the NMV

contains a microslide labelled “Halecium, Grif-

fiths Point, July, 1880" with one small infertile

stem identical with the Pearson J, specimen,

and the hydrophores of this stem show « very

clear rung of punctae between the margin and

diaphragm.

This is probably a new species, but due to

ils similarity to HW. ¢enellam its identity is in-

determinate until adequate Fertile material is

found.

Halecium sp. 2.

FIG. 14

Record: R, 35 m, on algae,

Murerial> Two yery small infertile stems.

Aydrerhize tubular. Stents unbranched, 2 mm

long, internodes of variable length, 0,28-0.66

rom, dian U.08-0,12 mm, perisare thick,

divided into segments by 2-3 deep, transverse

constrictions, the last segment expanding

slightly to support base of hydrophore. Hydre-

phore very shallow, depth to diaphragm 0,03

mm. Margin circular, 0.14-0:17 mm in diam.,

slishtly everted. Succeeding stem internodes

arising just below hydrophore, standing out

perpendictilarly, giving siem a zig zug appear-

ance. Hydranth too large to retract into hydro-

phore, body thick, about 24 stubby tentacles,

Remarks: All the bydrathecal margins are so

damaged that it is impossible to determine if

punctae are present, Although the dimensions

fall well within the range of J. lartkesteri

(Bourne, 1890) (Millard 1968, p, 257) the

internodes show no tendency to curve upward,

nor is there any sign of the secondary hydro-

phores common in this species. For these rea-

sons, the present specimens are not assizned to

A, fankestert.

Family SYNTHECIIDAE

Svyothecium elegans forma subveniricasum

Bale, 7914, Ralph, 1958: 347, fis. 16,

FIGS, 15. 16

Synthecium elegans Allman, ($72: 229, Black-

hurn, 1942; 111.

Synthecium subyentricosum Bale, 19)4az 5, pl.

1, figs. 3-5; 1915: 265,

Records; R, 34 m, on Herdmenia memeasy

S, 18-25 m, on stem of Therocerpuy eivuri-

catus var. eystifera; Stn. F, 65 m,. on worm

tubes with Diphasia subcarinate

Marerial: Several immature colonies: one fer-

tile stem. Stems monosiphonic, flexuons, to 2

cm long; no secondary branching, but a few

tendrils given off distal ends of hranches, Proxi-

mal stem internodes with 1-3 pairs of opposite

hydrothecae; succeeding internodes 1,5-1.8

mm long, a pair of opposite hydrothecae in

middie of internode, und u pair of opposite,

distally situated hydrocladia. Aydrothecae of

variable shape, generally tubular. three

quarters of length adnate to intemode, free

adcauline wall 0,07-0.15 mm Jong, fixed wall

0.42-0.45 ram: abcauline wall 0.58-0.44 mm

long. A delicate internal sheath clearly visible

i many hydrothecae, Murgin of hydrutheca

sinuous, sligbtly everted, O18-0.19 mm in

diam., a few marginal rcduplications. Gero-

theca—a single immature individual prowing

from the orifice of one of the second pair of

hydrothecue on basal stem internode. Calour

—white, with trace of purple.

Remarks: The single immature gonothecs iden-

ties the Pearson J, material with 8, swhvenrri-

casum Bale. recognised by Ralph (1958) as a

varietal form of §. elegans Allman,

168

JEANETTE BE, WATSON

Zygophylax antipathes (Lamarck). Portion of branch showing hydrothecae with everted

margins and regenerated hydrothecal pedicels,

. Ophiodissa blackburni n.sp. From holotype. Fig, 10—Hydrorhiza and stem with secon-

dary hydrophorcs and reduplicated margins. Fig. 11.—Reduplicated hydrophores, en-

larged Fig. 12.— Nematothecae, enlarged.

Halecium sp, 1. Whole stem, showing growth habit.

Halecium sp, 2. Part of stem showing hydraphores and growth habit.

» Synthecium elegans forma subventricosum Bale. Fig. 15—Part of stem. Fig. 16—Imma-

ture gonotheca.

. Synthecium dentigerum Jarvis, Fig. 17W—Part of branch with subupposite to opposite

hydrothecae. Fig. 18—Hydrothecae enlarged, showing internal adcauline teeth.

HYDROIDS 149

Although there is considerable variation in

shape of the hydrothecac among the specimens,

most aré tubular and closely adnate to the

hydrocladium, not ventricose, as described by

Bale for his specimens from the Great Austsa-

lian Bight, Morcoyer, there is only one pair of

opposite hydrothecae in the middle of each of

the distal stem internodes, and a pair of oppo-

site. distal hydrocladia, and the hydrothecal

marvins are decidedly sinuated. all features

considered by Bale to be criteria distinguishing

S, parulum Busk.

Thus, S. vlegany forma subventricasiuint may

eventually prove to be a synonym of 3. pata

lum. However, in view of the lack of adequate

fertile material, the fact that the typo of &S.

patulernt is not known to exist, and the possi-

bility that sexual dimorphism may occur, it is

hest to keep the species separate at present.

Syutheciurt dentigerum Jarvis, 1922: 344, pl,

25. fig. 15. Totton, 1930: 172. Millard,

1944-24. fig. 6,

FIGS. 17, 18

Records: S, 23 mon stem of Sertnlaria un-

gaiculata and Meramenntig momus

Marerials Five infertile stems, to 2 em long.

Stas monosiphonic, basal internodes fong..

3443.6 mm, with 5 pairs of opposite hydro-

thecac: each succeeding internode with 2-3

pairs of hydrothecae in mid region, followed

by a pair of opposite hydrocladia. Aydrocladix

ansing perpendicular to stem from a distinct

proximal joint; unustomoses. and some secon-

dary branching oceur, Aydrorthecue almost

titbular, adnate for two thirds their length,

fixed adcauline wall 0.45-0.51 mm long. free

wall (.15-1.2 mm: abcauline wall 0,36—-0.42

mm. Murgin narrow. sinuated, with slightly

everted cim, 0.21-0.27 mro in diam. Proximal

hydrocladial hydrothecae subalternate, hecom-

ing opposite distally. {One stem has alternate

hydrothecae with the abcauling wall hent

sharply outwards.) Adcauline submarginal

tooth present in most hydrothecae, variable

from wedge-shaped to a mere thickening of the

udeauline wall, No ahcauline teeth or marginal

teduplications,

Remarks: Three specics of Synthecine with

internal teeth have been described. §. carinassei

Totton, 1930, 8S. singulare Billard, 1935, and 8.

dentigeriuim Jarvis, 1922. The Pearson [. speci-

mens are larger than 8, carinatum and smaller

than 3. wingulere, but fall well within the range

giver by Millard (1964) for S. denligernen.

The specimens are distinguishable from S$. ev.

guns forma sithventricosum Bale, from Pear-

son 1, only by the presence of the internal suts-

marginal tooth, which is however not

developed at all in some hydrothecae, the most

prominent tecth being associated with those

hydrothecae which have a flexure of the ab-

cantine wall, Although the present matertal

differs in. some respecis [rom desenptions of §,

dentigerym in size of the colonies and arrange-

ment of dhe stem hydrothecne, these are neither

sulfigicntly constant nor importam characters

to Wattant the erection of a new species,

This is the first record of S. dentiveruen from

Austrahan waters. It has been reported twice

previously, from the Indian Ocean pnd South

Africa.

Fumily SERTULARRDAK

Thyroscyphus marginatus (Bale, 1884), Bale,

1915; 245, Stechow. 1925: 217. Black-

burn, 1942: 112.

Campianularia marginata Pale, 1884; 154, pl. 1,

fig, 2; 1888; 758: 1914) SI. Bartlelt, 1907: 42.

Records: R, [4-30 m on algac and sponge;

5, 22-30 m on Sergewsum varians

Material Four infertile colonies ot u few stems

each. Aydrorhiza a simple tube, lagsely wound

on substrate. Sven simple, to 1 cm lung,

smooth or slightly anoulated, diam. increasing

distally, a distinct transverse joint just shove

junction with hydrorhiza, Pedicely of hydro-

thecac 1.95-2.7 mm long, 0.25 mm in «liam

distally. In one stem, 2 branches ate given off

side by siule, 1 short, terminating in a hydro-

theca, the other continuing normal growth. giv-

ing off a pedicel distally. Hydrothecal marain

with +4 teeth, 4 valved operculum, and

thickened submarginal ring, Depth of hydro-

theca, 1.5 mm: diam. at margm, (.73-1-21

min.

Remarks: This agrees fairty well with descrip-

tions of T. marginatus given by Bale.

Parascyphus simplex (Lumouroux, 1816).

Blackburn, 1942: 112, Ralph, 1961a; 755,

fiz. 1. Stechow, 1925; 224.

Laomedea simplex Lamouroux, 1816; 204.

Cumpanularia siraples (Lamouroux). Bale,

1884: 58.

Pantponaitaris raridentata Hale. 1894" 98, pl, 3,

&, 3,

Tivrascyphus simplex CLameureux), Hodgson.

1980; 10, fiz, 22.

Records; R, 34 m, on sponge and Aere-

maria moms on vertical walls; § 25 m, an

Thecocarpus divaricarns,

Murerial) A few infertile colonies, Sreme short.

unbranched, t9 5S mm long. Averothecae

170

swollen on proximal adcauline walls same with

a short pedicel, Stem apophyses pronounced,

many with a constriction marking the site of

growth regeneration after breakage.

Remarks: The stem apophyses figured by Hudy-

son (1950) and Ralph (1961) appear to merge

into the base of the hydrothecae, Bale’s (1894)

figure shows a more pronounced apophysis.

similar to those of the Pearson TI. specimens.

Diphasia subcarinata (Busk, 1852). Bale, 1884:

102, pl. 4, fig, 1. pl. 19, fig. 18; 19144; 7;

1915; 264, Ritchie, 1911; 850. Hodgson,

1950: 20, figs. 34. 35. Ralph. 1961a: 764.

fig. 5, Shepherd & Watson, 1970: 140.

Serratia sithearinata Busk, 1852 390,

Records; R, 20-34 m on bryozoa; 8, 25 m

on Amansia pinnatifida and Herdimania

mranuiss Str. F635 m, on worn tube.

Maretialy Many infertile unbranched colonies

0.5-1 em high. C'oleur—dark brown.

Remurks: ‘The keel deseribed by Bale (1884)

in his Victorian material is ptesent in the Pear-

son [. specimens only as an indistinct ridge

passing between the Jateral maryinal tooth and

the adewuline thecal wall. Ralph (1961) notes

the presence of the ridge as a “prominent fea-

ture” un her New Zealend specimens, but

Hodgson (1950) was unable to find the ridge

in his. Tasmanian material.

Stercatheca elongats (Lamouroux, 1816).

eae Lene, 23. figs. 38, 39, Ralph,

1961: 762, fig. 4. Shepherd & Watson.

1970; tag

bert itaria sian Lamouroux, 7816: 189, pl,

Bale, 1884; 75, pl, 6, figs. 7, 8 pl 19, re,

7: 19)3: 277. Mulder & Trebitcock, 19t4a; 3,

pl, t, figs, 7-10.

Records: R, 30-45 m; S, 12 m, of Srene-

claudia australis, Phacelocurpus lahillaradiers,

Scvrathalia dorvearpa and Aerovarpia pani-

culdta.

Materiel: luxuriant colonies, some fertile.

Sremy 4-5 cm long, Gonothecae with long

horned processes.

Remarks: §. clangata is one of the commanest

epiphytic hydroids of the southern Australian

coastlins. The Pearson f. specimens correspond

to the “short stemmed ocean form" of Mulder

& Trebileoek (19148). 8. eloneuta shows a wide

choice of algal substrate and consideruble

tolerance of environmental conditions. The

stems of the present specimens Were fice of the

encrusting coralline alga usually axsocinted with

this species,

IFANETTE k, WATSON

Crateritheca sacanthostoma (Bale, 1882),

Ralph, !96la; 756, fig. 2. Shepherd &

Watson, 1970: 140. Millard, 1964; 26,

fig, 7.

Sermlaria ariel embeeeis rn 1882; 23, pl £2.

Fig. 4; R84: 8&5, pl. 4, figs. 7. 8: 1973: 434.

Bartlert 1907; 44, hile * Trebileock, 1914)

Stereotheed acanthesionta (Bale), Stechew:

1919; 103. Blackburn, 1942. 112.

Records; R, 24-33 mm. of sponge and red

algae,

Material: Two colonies of 4 few stems each.

Stenisto 32cm long,

Remarks: The Specimens agree exactly with

Bale’s description of 3, acanthosrania.

Crateritheca crenata (Bale. 1854),

1941a: 757, fig, 2.

FIG. 19

Sertalaria crenata Bale, 1884: 86, pl. 4, fig. 2.

Record: R, 33 m, on brown algue.

Material: Two fragmentary infertile stems.

Hydrorhiza tubular, winding. Sten fragments

2.em Jong, with 4-6 deep proximal annulations,

followed by a short athecate internode below

first branch, Internodes 0.13-0.26 mm_ tong.

0.04-0,06 mm in diam. ai node.

Remarks: The Pearson 1. specimens have a

much less pronounced outward bend of the dis-

tal thecal wall than C. crenara figured by Bale

(1884), However, a microslide of C. cremara

trom Snapper Point, Vic. in the Bale collection

of the NMY, compares very closely with the

Pearson [. material.

This is the second record of the species, and

4 new record for §, Aust. (Other locality—

Port Phillip Bay. Vic.)

Salacta obliquanoda Mulder & ‘frebilock,

1914).

Ralph,

FIG. 20

Sertularia obliqtanoda Mulder & Trebilcock,

(9)3b: 41, pl. 5, fig, 1, Stechow, 1924; 106.

Shepherd & Watson, 1970; 140),

Records: R, 18-46 m, on several species of

red algae, including Metunnstophora flabel-

leva, bryozoan, und sponge,

Meverial; Luxuriont colonies. — Epiphytic

colonies fertile, Aydrerhiza loose, tubular.

Stems simple, to 8 mm high, some giving olf

distal tendrils which form new stolons, Stem

Interrodes variuble in length, 0.54-0.46 mm.

width at base of hydrotheca, 0.18-0.24 mm.

joints oblique, best developed on short inter-

nodes, indistinct or absent on long internodes,

Hiydrowivese similar to the description given

ELYDROIDS Wt

by Mulder & Trebilcock, but the hydrothecal

aperture is oblique, mot vertical, sloping

diagonally back towards the stem in a line:

parallel with the abcuufine wall. Length of free

adcauline wall 0,12-0.18 mm, fixed adcauline

wall, 6.24-0,27 mm, abcauline wall, 0.21-0.30

mm long. Margin with 2 shatp adcauline teeth,

and q thickening of thecal wail in the base ot

the abcuuline sinus; width of margin 0.06-0.15

mm. Gonothecae large, barrel-shaped, |-53—

1.6 mm Jong, 0.96-1.06 mm wide, with 6-8

deep annulations, a circlet of hooked teeth be-

law tim. Usually 1 gonotheca on a stem, borne

helow the proximal hydrotheca; male and fe

male gonophores on the one colony,

Remarns; With the exception of the somewhat

longer stem internodes and more oblique aper-

ture, the Pearson I, specimens compare closely

with the type of Sertu/uria ebliqvaneda in the

collection of the NMY.

Blackburn (1938, p. 31% 1942. p. 113)

listed Dynamena cornicing McGrady, 1858,

among the hydroids of the Sir Joseph Banks

Group, D. cornicina (=Serrularia complexa

Clarke, 1879) (see Bale 1885, p. 769; Billard

1925, p. 1838) and S& obliquanods are very

similar, and are difficult to distinguish oxeept

in fresh fertile material. However, the hydro-

thecae of D. cornivine ave larger, and the aper-

tural teeth are more Jalerally situated, The ab-

cauline opercular flap, easily visible in the

present material. clearly distinguishes 5. obfi-

quanode frum D. carnicine.

The present apecimens also resemble Triden-

tara rurbinata ({Lamouroux, 1816) (Stechow

1925, p. 223) particularly in the presence of

the abcauline fiap ond the thickening of the

abcauline wall. ‘The status of this group needs

further elucidation,

S. obliqnanade is one of the commonest

species in the collection, This is the first

definite record of S, ebliavanada for S. Aust,

(Other localities—Torguay and Barwon Heads,

Vic, }

Sertularella robusta Coughtrey, 1876; 300, fig.

22: Blackburn, 1942; 115. Hodgson, 1950:

33, fig. 53. Ralph, 19la: 824. fig. 22,

Shepherd & Watson, 1970: 140.

FIG, 71

Records; R, 24-33 m: S, 15-24 m, on Ballia

callitricha, Laurencia elata. Herdmania

momus, bryozou. and sponge,

Marerial> Numerous infertile colonics, Stems

simple, iinbranched, te | cm Jong, arising fram

a tubular fydrerhiza, Stern internodes variable

in length, O.42-1,14 mm, but fairly constant in

moimum width, 0O15-0.18 mm. measured

just below hydrotheca. Aydrothecae distal on

jong internodes, occupying most of the length

of short internodes. Length of free adcauline

wall 0.3 mo, fixed adcauline wall 0.24 mm;

abcauline wall 0.42 mm; maximum width af

hydrothees, 0.24 mm. Thecal walls moderately

to faintly annulated with 2-3 broad undulations

passing around widest purt of hydrotheca.

Remarks: Following Ralph (1961a), Lhose

stems with a fairly thick perisare aid annulated

thecal walls, even though the unnulations may

be Faint, are assigned to S. robaester.

Sertularella simplex (Hutton, 1873). Ralph,

19fla; $21, fig, 21.

FIG. 22

Sevtularia simplex Hution, 1873; 257.

Sertulerella peregeina Rule, 1926; 19. fig, 4.

Records: R, 30 m, on the stem of Thece-

carpus divaricatus var, cystifera, Herdmania

momus, and on bryozoa.

Material: Colonies of a few Fertile stems, Streams

to 1 em long, occasionally branched, arising

from a tubular hydrorhiza. Stems smouth,

proximal internode athecate, with a few in-

definite snnulations, nodes distinct, sloping al-

ternately right and left, Internodes fairly tong,

0.39-0.60 mm, becoming progressively shorter

distally, until hydrotheca occupies about two-

thirds of internode. Width of internode below

hydrotheca, 017-020 mm. Branches, when

present, arising just below the hydrotheca, the

first branch internode with 2-3 annutations.

Tendrils present, growing from the distal ends

of stems and from broken hydrathecae. Hydro-

thecae with 3 internal submuarginal teeth—l

#beauline, 2 adcauline; thecal walls thin and

smooth, length of free adeauline wall variable,

0.33-0.40 mm, fixed wall, 0.25-0.27 mm;

abcauline wall, 0.52-0,54 mm: maximum width

of hydrotheca, 0.22-0.27 mm. Margin showing

occasional reduplications,

Remarks; The material from Pearson I,,,

although variable, falls well within the cange

of variation of S. simplex defined by Ralph

(1961a). The specimens assigned here to S.

simplex are easily distinguished from 4, rehbuxia

from Peurson 1, by the generally larger and

smoother walled hydrothecae-

Bule (1926) erected Sertnfarella peregrina

to include hydroids from Bass Strait and Port

Phillip formerly referred to Sertularella paly-

zonias und S. guudichardi. S. peregrina is indis-

inguishable from §. simplex as now defined,

72 JEANETTE

accordingly S. peregrina is here referred te the

synonymy of S. simplex.

A new record for §. Ausr.

Sertularellu annulaventricosa Mulder & ‘Trebil-

cock, 1915: 34, pl, 7, fig 1, pb 8, fig. 4.

FIG. 23

Senilareta undulata Bale, 1915: 284, pl, 46,

Hig. ). Hodgson, 1950; 34, fig, 59,

Records: R, 33 m, on Sarpaysunt sp., on red

algae, und bryozoa.

Muterials Colonies moderately abundant, infer-

tilt, Hydrorhize wubular, Siems simple, to 5mm

long, with 2-4 hydrothecae (exceptionally, i

stem has 10 hydrotheeae; another is branched)

hut. many hydrotheeve arising singly from

hydrorhiza, Stems annulated proximally, annu-

lafions extending to buse of first hydrotheca,

{nternedes 0.30-0,51 mm long, width helow

hydrotheca, 0.18 mm. /lydroecaue barrel-

shaped, 0,27-0,36 mm in diam, at widest part,

Margin 0.15-0.24 mm in diam., depth trom

margin to base, 0.30-0.36 mm.

Remarks: The holotype microslide of S. annti-

laveninicesa in the collection of the NMV has

longer stem internodes than the Pearson I.

specimens, and is unbranched, although Mulder

& Vrebilcock note that “one specimen shows

signs of having been slightly branched”. Vhe

hydrothecal walls of the type are fairly. smooth.

with w ledge passing around the hydrotheca u

little below the margin. The walls uf the Pear-

sou 1. specimens are not a3 smooth as these af

the type, and the submarginal ledge is replaced

by I-2 annular ridges. giving the hydrotheca a

crumpled appearance. As in the type material,

the aperture of the present material is some-

what variable in diam., ranging from 4 narrow

orifice ta almost the complete width of the

hydrotheca-

‘This is the third record of the species, and

a new récord fur S. Aust. (Other loculities

central Victorian coastline, ancl Tasmania).

EF. WAISON

Sertulurella ayrilia n.sp.

FIGS, 24, 25

Type Maternal and Records: Holotype, NMV

GI%64, microslide; paratypes, Gi96S,

G1966, G1967, inicroslides; SAM H35,

microslide; holotype and paratypes from 8,

13 m, On Sergessunr verruculosum.

Dexerigtion from holotype ana puraly pes: Stems

simple, short, to 4 mm Jong, unbranched, aris-

ing from a thin tubular hydrorhiza. First stem

intetnodes short, with 3 proximal annulations:

succeeding internades of variable length, 6.32—

0.53 mm, widening from w narrow oblique

proximal node, 0.04-0,.08 mm in diam, te base

of hydroiheca. Nodes sloping alternately left

and right, with I-2 oblique annulations, re-

mainder of internode smooth, Mydrothecae dis-

tal on internode, alternate, a. maximum of &

on stem, each sloping outwards parallel with

line of internode, giving stem a zig zaz appear-

ance. Body of hydrotheca long, almost. cylin-

drical, slightly swollen at junction with inter-

node. 016-019 mm in diam. Adcauline wall

with 5—7 uniform, rounded annulations, most

prominent across widest part of hydrotheca,

but reduced to 4-6 on abcauline wall, fading

out proximally. Adcauline wall arched out-

wards, abcauline wall inflexed into .a long, nar-

tuw neck, 0.10-0.20 mm at narrowest dian,

expanding again to margin. Length of free ad-

cauline wall, 0.36~0.45 mm, fixed adeauline

wall. 0.12~0.14 mm; abcauline wall, 0.32-0.37

mm. Aperture facing outwards and slightly

down. Margin, 0.11-0.14 mm in dian, with

4 broad, low teeth, the adcauline tooth most

prominent; 3 strongly developed internal sub-

marginal teeth in theeal neck—2 identical

dorso-lateral bract-like teeth, and | long peg-

shaped sbcauline tooth. Ayedranth — in-

sufficiently preserved for description, but shows

evidence of an abecauline caecum. Gonethecu—

1 immituce individual, arising from the base

SK SSeS

One stem jnternode showing hydrothecac

Fig. 19. Craterithecu crenata (Bale). Part of branch with three hydrothecae.

Fig- 2d, Salieia ebliqnanoda (Mulder & ‘Trebilgock),

with abcuuline opercular flap.

Fig. il Serlaretla robusta Coughtrey. Part of stem showing hydrothecae with shallowly anniu-

lated walls, and hydranth with abcauline caecum,

Fig. 22. Seetularclla sitnplex (Wutton). Part of stem showing smooth-walled hydrothecse:

Fig, 24, Sertularella annulaventricosa Mulder & Trebileock, Pact of stem.

Figs. 24.25. Sertularella avrilia m3p. From holotype, Fig, 24.—Whole stem. Fig, 25,—Part of stem,

enlarged, showing hydrothecac and internal submarginal teeth,

Fig, 26, Seriularetia sp. 1, Whole stem with two hydrothecae,

Fig. 27. Sermlaretla sp. 2. Part of stem with two hydrothecue,

Figs, 28-90. Symplectoyesphus vostratus tsp. Big. 28.-

Stem with one hydrotheca and ponotheca,

from holotype colony. Fig. 29.—Stem with two hydrothecae: from paratypes, Fig. 30-—

Hydrotheca, lateral view, showing internal submarginal teeth, from paratype.

174

of a proximal hydrotheca; body strongly ribbed,

with signs of the development of a slender ter-

minal neck and 4 blunt spines.

Remurks: &, aveilia resembles both 5. roluse

(Couhtrey, 1876) and S. gilehristi Millard,

1964. However, 3. aveifia is smaller than S.

robusta, the hydrothecae jee more strongly

anuulated, and it is further distinguished by the

long, curved thecal neck, Although S. evrilia

shows some affinitics with S. gilchrisri, this

Seuth African species is a larve, branching

form, with fascicled stem, and a shorter, Icss

conspicuously arched thecal neck,

Sertulurella sp, 1,

FIG. 26

Revords: R. 21-33 m, on Lawreneia elata,

Herdmania momus, Halopteris campanuia

var. campattula, and bryozoa.

Material; Numerous infertile colonies, Stems

simple, monesiphonic, unbranched. straggling.

arising from a tubular hydrorhiza 6,05 mm in

diam, Stems 10 3 mm long, first stem internode

short, with 2-3 indefinite annulations, following

internodes thecate, of variable length, O0.06—-

0.24 mm, irregularly annulated except just be-

low hydrotheca, Nodes distinct, sloping alter

nately right and Jeft, 0.04-0.06 mm in dian,

measured just below hydrotheca, Aydrothecae

distal on internode, a maximum of 4 on stem:

body of tfydrotheca barrel-shaped, one third to

one half free of internode: Jength of fixed ad-

cavline wall, 0.11-0.14 mm, free adcauline

wall, O.15-0,24 mm) abcauline will, 0,25-0,34

mm; maximum width of hydrotheca at junction

of udeuuline wall with internode, 0.20 mm,

hydrotheca gradually narrowing to margin.

‘Thecal wall with S—7 strong, entire annulations,

most marked in mid-region, annulations fading

out towards margin, Margin variable in diam.,

0,08-0.13 mm, with 4 sharp, equidistant tecth,

Nydranth with abcauline caecum, Colaur—

yellow-brown.

Remarks; The species resembles §. angulosa

Bale, 1894 (= S. robuyta Ralph, 1961) but is

a smaller species, with much more deeply in-

cised thecal ridges. [t is further distinguished

from §. rebusta by its straggling growth habit

and the large oumber of hydrothecse arising

directly from the hydrorhiza.

Although displaying » wide choice of sub-

sttate, occurring on algae, ascidigns, hryozoa,

und other hydroids, this Sertutdrelld was

recorded only on the exposed site, where is was

very abundant.

JIEANKTTE B, WAISON

lt seems likely that this is 2 new species,

tut is indeterminate until fertile material is

found,

Sertularetla sp. 2.

FIG. 27

Record: R, 18m, no substrate recorded.

Marerial; Threc fragmentary infertile stems de-

tuched from the hydrorhiza, Stems straight, un-

branched, occasionally bent slightly at u node,

pensare very thick und brittle, Intemodes of

variable length, 0.48-0.96 mm, nodes oblique.

sluping alternately lefrand right, angle of slope

variable, Internode narrowest at node, 0.18-

0.24 mm in diam., followed by 1-2 proximal

annulations, widening to base of hydrotheca;

width of internode at base of hydrotheca, 0.27—

0.36 mm. Hydrothecae occupying distal half

to two-thirds of internode, sfanding out at about

30)° to axis, very large, variable in shape, either

cylindrical, or with a slight distal narrowing be-

hind margin, 5 distinct annulations passing

completely around hydrotheca, the strongest in

the mid-region of the abcauline wall, fading

out proximally, annulations Jess distinct on

alder hydrothecue, Length of free adcauline

wall. 0.39-0.48 mm, fixed adcauline wall 0.36—

0.45 mm; abcauline wall 0.66—-0.72 mm. Mar-

gin O.33--0.51 mm in diam.. thickened, with 4+

low, blunt, slightly everted teeth. Operculum

of 4 flaps. Hydrenth not well preserved, but

an abcauline caccum may be present.

Remarks: The hydrothecae are distinctive in

shape, and are the largest recorded in Austra-

lian Waters for Sertularella. This is almost cer-

tainly a new species, but confirmation nist

awail the collection of adequate and fertile

material.

Symplectoscyphos Jongithecus (Bale, 1883).

Sertularella longithecu Bule, 1888: 762, pl. 16,

fie. 5, 6; 1894: 101, pl 4, figs 7-9.

Record: Sta, F, 65 m, no substrate recorded.

Murertal: A few straggling infertile branched

stems to ¥ cm Jong. Stem internodes straight.

0.54-0.75 mm long, nodes well defined, slop-

ing alternately right and Jeft. Branches given

off from front of stem opposite base of hydro-

thecu. Hydrothecue Jong, tubular, narrowing

distally towards margin; length of free adcau-

line wall, 0.244036 mm. Margin, 0.15-0.18

om in diam, One hydrotheca shows regenera-

tion after breakage at base.

Remarks: The Pearson I, material compares

well with Bale's (1888) specimens from Port

Dennison and Port Phillip Bay. bat they have

HY DROLDS

a shorter length of hydrotheca free of the inter-

node than Ritchie’s (1911) specimens from

Wata Mooli, N.S.W.

This is only the fourth record of this

ipparently rare deeper water species, and a new

record for S. Aust,

Symplectoscyphus sobdichotomes (Kirchen-

pauer, 1884). Ralph, 1961a: 813, fig. 20,

Sertnlarelia suhdichatoma Kirchenpauer, 1884:

46, pl. 16, fig, 1. Bale, 1Y¥I4a: 20 (discussion).

Records: R, 30 m, on bryozoa; Sto. F. 65

m, on bryozoa,

Marevial> Two colonies, each of a few infertile

stems. Siemy straggling, to 4 cm long, alter-

nately, but irregularly branched. Nodes present

on stem and branches, stem internodes indis-

tinct, 1-3 annular constrictions at junction of

hranch with stem: several branches terminating

in tangled anastomoses. Hydroshecae somewhat

conical, with & slight concavity in middle of

abesuline wall; a fine diagonal line running

From the base of the adecauline wall to a small

internal pee in the flexure af the abcauline

wall,

Remarks; The Pearson |, specimens compare

closely with microslides of Sertularefla divari-

cata from the Great Australian Bight in the

collection of the NMV (Bale 1914a. p, 20).

Svmplectoscyphus neglectus (Thompson, 1879).

Shepherd & Watson, 1970; 140,

Sertutlarella neglecta Thompson, 1879: 100, pt,

15, fig. 1. Bale, 1884: 110. pl. 3, fig. 3, pl. 19,

fig. 22, 23; 1915: 287. Blackhurn, 1942: 115,

Syinnlectoseyohus sp. Ralph, 1966: 163, figs.

Records: R, 25-30 m, on Delivea pulehra,

Metaconfolithon charoides, and other red

and hrown algae.

Material: Luxuriant fertile colonies. Stems to

2 om long, beginning with 2-3 oblique proximal

twists, branches suballternate, no secondary

branching, but occasionally a branch produced

into a tendril. Hydrothecae triangulat in see-

finn in young stems, with 3-4 distinet annular

ridges, thecal walls of mature specimens much

thickened and rounded, the annulations less dis-

tinct: marginal teeth of younger hydrothecae

long and sharply pointed, blunt in older speci-

mens. One-3 smal) internal submuarginal teeth,

sometimes not developed, but in mature hydro-

theeae may be thickened and projecting into

centre of cell, Gonorhecae abundant, male and

female on separate stems. Female gonophores

borne thickly on stem and proximal part of

branches; male gonophores bome only on mid-

175

region and distal part of branches, Both sexes

on a short pedicel arising beside a hydrotheca;

hady with 10-15 annulations and 2 hollow.

conical distal processes. Female gonotheca

stout, inflated, widest near middle, blastostyle

spindle-shaped, supporting 4 cluster of ova.

Male gonotheca long, narrow, widest near base,

with a short distal obliquely inclined neck,

blistostyle thin, rod-shaped, becoming indis-

tinet distally.

Remarks: Bale (1884) in his redescription of

8. neglectus, had only dried material before

him, and inferred the transversely wrinkled.

tiangular hydrothecae to be artifacts of drying.

However, much of the present material, par-

ticularly the younger stems, shows this to be

anormal character of the species.

Bale’s surmise that 8, neglects would show

sexual dimorphism is demonstrated hy the

Pearson I, material. His figure “a” (PI. XTX,

fig, 23) with “two latge conical hollow teeth,

one more elevated than the other” ts a female

gonotheea, and gonotheca “h" (fig. 22) with

“teeth smaller and about equally elevated” is

male. Tn the Pearson lt. material, the tooth-like

conical processes of the female gonothecae are

of approximately equal hetght, while those of

the male are of unequal length and fairly short,

hat this is variable througheut the range of

specimens. Ralph (1966) described and figuied

Symplectoveyphus sp. (from Port Phillip

Heads) with smooth hydrothecac of triangular

section and sharply erect marginn) teeth.

Although the hydrothecue are smoother than

usual, the two latter characters clearly distin-

guish her material as young specimens of S.

neplectus,

5S. neplectus is a very common epiphytic

hydroid in southern Australian waters, occurr-

ing on a variety of algae, Ii is easily recusmised

in the ficld by the incurved habit of the

branches, the encfustation of pink coralline

ilgae usually present, and the bright ycllow

gonothecav. The short marginal teeth seen on

alder hydrothecac are probably the result of

constant abrasion against other slems and algae

in the very turbulent conditione in which it is

usually found.

Symplectoscyphus indivisus (Bale, 1882).

Raiph, 1961a; 803, fg. 15. Shepherd &

Watson, 1970: 140.

Sertataretia indivisa Bale, 1882: 24, pl. 12, fig,

7; (8&4 105, pl. 3, fig, 4, pl 19, fig, 27; 1915-

285, Biackburn. 1942: 115.

Records; KR, 21-45 m, on Lauretivia elata

aml Sargessam spinuligerum: S$, 12-30 m,

176

on Sargessan spp, Déistreniiune sp. and

Polvsiphenia sp-

Material: Colonics abundant, 1 colony tertile,

growing from a loosely wound hydrorhiza.

Stems to S mm long; gonothecae clustered

thickly at base of stems. Colour—bright yellow.

Remarks: The colonies fall within the known

range. of variation of S. indivisus, but are

separable into 2 distinet morphological

groups. The first group comprises stems with

short, strongly undulated internodes, often com-

pletely occupied by the hydrotheca, The hydro-

thecae are inflated, irregularly undulated. with

a short submarginal neck, The gonothecae are

squat, deeply crumpled, with very short pedi-

vel, This group compares with Bale’s (1888)

5, fudivisa trom Portland, Vic. and figs. 5. 6, of

§. varigbilis from Port Jackson. N.S.W. The

neck region of the Pearson [.. specimens are

however, more contracted than those figured by

Bale.

The stem internodes of the second group are

longer. and both internodes and hydrothecie

are less inflated. than those of the first group-

The thecal wall is only occasionally faintly uo-

dulated, and the neck region Is longer, The

colonics ure infertile.

There ws thus a goal correlation between

stem morphology and environmental condi-

tions. as the robust fertile) stems were found

only on the rough-water site. whereas the mure

ficxuous (infertile) stems occurred only on the

sheltered side of the island,

Symplectoscyphus pygmaeus? (Bale, 1882}.

Serrvlarctla premaeus Bale, 882: 25. pl, 12,

fig. 4; 1884; LOS, pl. 3, fig. &. pl. 19, fie. 19.

Biackilrn. 1942: 115, Hodgson, 1950: 3h, figs.

63, 64,

Symplectoveyphus pygmaeus (Bale). Ralph,

1961a: £05, fg. 16.

Records: R, 18-30 m, on Herdmania

moms, bryozaa and compound ascidians:

§, 18-24 m. on stem of Thecocarpus divari-

cafes var. eystifera,

Marerial: Infertile colonies comprising a few

stems to 4 mm long. Coleur-—hright yellow,

Remarks: It is difficulr to distinguish between

infertile muteriul of S. pygmaens and &, ren-

roni (Bartlett. 1907), Ralph (1961) distin-

guishes between the two species on the line of

fine dots passing from the base of the adeauline

wall to a point one third the distance up the

abcauline wall in S. pygmaeus, and a lower

diagonal in §. renton?, However. examination

of a series of microslides of 4. pygrnenty in the

collection of the NMY, shows that this is not

JEANETTE E. WATSON

a reliahle distinction, as the height of the

diagonal varies considerably betweem different

stems, and even among hydrotheeae on the

same stem.

Most of the hydrothecae of the Pearson 1.

matenal have # ling of dots joining the ab-

cquline wall about one quarter the distance up

from the hase, a distance vreater than that

given by Ralph as diagnostic for S$. pr prices,

the junction being marked by a thickened noich

on the inside of the wall, As the Pearson I.

specimens most closely resemble 5, pyenraens,

especially one slide in the Bale ¢ollection

(NMV} labelled “Queenscliff, 1881", the speci-

mens are provisionally assigned to this species.

Symplectascyphus macrothecus (Bale, 1882).

Shepherd & Watson, 1970; 140,

Sertulerela mavrofhecn Bole, (882); 25. pl 13.

fig, 1; 1X84; 107, pl 3, fe 4. pl 19. fig. 24.

Bartlett, 1907: 65, fig.

Records: R, 24m, on Acrocarpia paniculate,

Materials One infertile colony of a few stems.

Hydroerkiza «a coarse: undulating tube, Sremi

to 4 mim long, robust, atheeate part very short.

with a strong distal constriction. Jnternades

conspicuously inflated’ behind hydrotheca,

nodes sharply twisted. Aydrothecue large, 2-6

on ster, completely occupying internode; fixed

adcauline wall 0.18-0.20 mm. free adewuline

wall 0.35-0.40 mm; abcauline wall 0.35-0.40

mm. Thecal wall smooth, with a noteh on sh-

cuuline side below margin, opposite the sub-

marginal tooth. Margin 0.15-0.20 mm in diam,

tnieral view, Three internal submarginal teeth,

the aheauline tooth best developed.

Remarks; The present material agrees well with

deseriptions snd figures by Bale of §. macra-

theca.

Symplectoscyphus rostratus 1.5p.

FIGS. 28-35

Type marerial and Records: Holotype, NMV

G1981. microslide--R, 27-30 m, on Surgas-

rum verruculosin, G2095, preserved miat-

eriul, remainder of helatype colony; para-

types, NMV GI982—R, 27-30 m. on Sar-

gauss verruenlusim: GAYSA—-R, 33 m. on

bryozoa; G1984—R, 27-30 m, on Surgayynnt

verruculosunr, mictoshdés: SAM H36——S, 46

m.on ted algac; microslide.

Descriptions from haletype and pérarypes:

iHydrorhiza tubular, loosely adherent to sub-

strate, Stems short, to 2 mm long, unbranched,

bearing I-3 hydrathecve, perisare thick and

brite. Stem internodes twisted, Inflared behind

HYDROIDS "iy

hydrotheca. proximal internode with 2-3 annu-

lations; width of internode at base of hydro-

theca O:.17-0.26 mm. Aydrotfycae alternate,

occupying most of internode, directed towards

front of stem. cach succeeding internode aris-

ing behind base of preeeding hydrotheca,

directed ovtwards, giving stem a zig-zag

appearance, Hydrotheca barrel-shaped, narraw-

ing ta margin, with 2-3 shallow annular ridges

passing completely around mid-region of thecal

wall, Depth of hydrotheea (from hase to mar-

gin) 0.42-0,50 mm; 0,27-0.30 mm. in diam. at

widest part. Margit contracted, small, rim

heavily thickened, with 3 tecth—1 blunt tooth

in the ceatral adcauline position, forming a

raised beak-shaped crest: 2 blunt. tow lateral

tecith, flanking crest. Abcauline side of margin

a shallow curve, Margin 0.12-0.16 mm in

diam. (lateral view). 1.10-0.13 mmr high (ad-

cauline embayment to crest). Aperture facing

obliquely outwards, depressed into the distal

ridge of the abcauline wall. Four internal sub-

Marginal teethe-2 adcauline, long, flanking

Taarginal crest, projecting downwards into cell;

I. low and ledge-ike (not well seen in an-

terior view) just below margin in the centre

of the abcantine embayment, and 1, similar in

shape, but smaller, deep in the adenuline side

of thecal neck. directly opposite the alcauline

submatginal tooth, seen only in lateral view,

Hydraeth with abeauline caecum, connected

by u delicate web to the abcauline wall belaw

the internal tooth. Gonothecae large, ovate, 0.8

mm long, 0.6 mm wide. arising from a short

pedicel hetow proximal hydrotheca, with 5

strong, crumpled annular ridges, and 3 low,

fairly sharp apertural teeth,

Remarks: The material of S. rastrams from

Pearson I. included only 2 gontthecae, one of

which was immature.

S, rostratus is in some Tespects transitional

between the smaller forms of 5. indivisns Bale,

and S$. snacresiecis Bale, resembling the former

in géneral aspect af |he trophosome and gono-

some, and the latter in the arrancement oF the

imMerrial submarginal teeth, There ts hawever,

only | abcauline submarginal tooth in S, ree

fratus, compared to 3 in J, macrotherus. fn ¥.

indivisns, the 3 mareinal teeth are alternate

With the tnaruinal teeth, The raised adcautine

crest further distinguishes §. resiralys.

Symplectuscyphus epiznicus n.sp.

FIGS. 31-33

Type Material and Records; Holotype, NMY

G1985, microsiide—S. 20 m, on Theco-

rarpus divaricanns van cvatifera; G2096, pre-

served material, remainder of holotype co-

lony; paratypes, G1986, GI9R7T, GLOSs,

microstides—R, 30 m, on TL divaricarer var.

evstifera; SAM H33, micrastide,

Description fram heletype and peratypest

Hydrorhkiza tubular, of same diam. as sterns.

Stems simple, short, unbranched, to 7 mm long.

Proximal stem mternnde short, athecate. with

4-5 annulations, width 0.13 mm; following

internodes of variable Jength. 0.50-1.05 iim,

ftydrorhecaé large, pecisarc delicate, alternate.

in one plane, a maximum of 4 on stem. nat

immersed in internude, distal on long inter-

codes, occupying almost the whole Jength of

short internodes, without definite floor. barrel-

shaped, widest about middle, narrowing only

slightly to margin. Leneth of fixed adcauline

wall 0.22-0.28 mm, free adcauline wall 0,21-

0,30 mm, ubcauline wall 0.45-0.53 mm. Mar-

gin O,28-0.31 mm in diam., thickened, with 3

equi-distant bluntly pointed tecth—1 edceuline,

2 lateral abeauline. Operculum of 3 delicate

flaps, No internal submarginal teeth. Hydranth

with approx. 24 tentucles, and an abcauline

cuecum, Gonetiecae large, ovale, neatly 3

times length of hydrotheca, 1.11-1.35 mm

long, widest at top. 0.87-1.02 mm, tapering to

a short pedicel arising below proximal hydro-

theca, walls fuintly undulated proximally. the

anmulations more distinet about mid-region.

Aperture small, circular, 0.13-0.15 mm in

tlam., depressed into the most distal annula-

tion of the gonéthecal wall; 4 very low rounded

teeth, Gonophores femule, mature, now filling

Pponothecal cavity, with 10-16 eggs, Colanim—

yellow.

Remarks; The colonies arise from a single sta-

fon running up the main stem and branches of

the host, the stems and occasional single hydro-

thecae given off at irregular intervals.

S. eplzeicus resembles one of the farger

forms of §,. indivisns (Bale) (ie. “Sernularella

feriahiliy’ Bale, 1838) in size and structure,

and could easily be confused with this species

in preserved material, However, S. epizotcus

lacks the internal submarginal teeth which dis-

tinguishes 5. indivisns.

Sertularia meacrocarpa Bale, 1884: &0, pl. 5,

fig. 2, pl. 19, fig. 11: 19l4a! 14; I19[5:

277, Mulder & Trebileock, 1914b; 42,

Hodgson, 1950; 27, fig. 47. Shepherd &

Watson, 1971: 140,

Records: R, 25-34 wy S, 4-25, anvone hol-

fasts of red algae.

178 TRANETTR F, WATSON

Material: Colonies abundant, growing in thick

tangled clusters. Stems us 12 cm long, infertile

except for | gonotheca. Colerr—dark hrawn.

Remarks: This distinctive species is easily

recognized by its dark colour, and large.

tangled! colonies which usually grow at the base

of ulgue in semi-sheltered situations.

Serfularia unguiculata Busk, 1852: 394. Bale,

L884: 76, pl. 6, figs. 9-12; L894: 100;

L9]4a: 16; 1915: 273. Blackburn, 1942:

113. Hodgson, 1950: 26, figs. 45. 46.

Ralph, 1961la: 788, fig. 13,

Records: 8, 25 m, on Herdmanta momus,

and among algal holdfasts.

Material; Several large infertile colonies. Stems

short. to 3.5 cm, unbranched, Proximal branch

internodes with 3 pairs of hydrotheeae, euch

succeeding internode with 2 pairs of hydrothe-

cae, nodes. indistinct. Ayedrothecae on branches

adnate for two-thirds of length; cauline hydro-

thecac not immersed in stem. Colour—orange

brown,

Remarks; Although shorter, the stems m the

present collection conform to Bale’s (1884)

description of the thick stemmed, long Inter-

node form of $, uaguienlate.

Although relatively common at Pearson L, 9.

wunrguiculata was restricted to sheltered water.

Sertnlaria bicuspidata Lamarck, 1816: 21.

Blackburn, 1937: 367.

Serthlaria bicornis Bale, 1882: 22, pl. 2, fig.

3) 1884: 83, pl. 5, fig. 9.

Records; RB, 45 m, on Rhodopeltis australis

und Metamastophora flabellata,

Material; A few infertile stems. Stems sttilty

erect, branched, to 1 cm long, Colour—dark

brown,

Remarks: The distinctive paired finger-like pro-

cesses flanking the margin distinguish this spe-

cies From all other species of Sertularia in Aus-

tralian waters,

This is the first undoubted record of §. his

cuspidara from S. Aust, (Other localities—

Queenscliff, and Lady Julia Perey 1., Vic.)

Sertularia maccallumi Bartlett, 1907: 62, fg,

Mulder & Trebileock. 19144: 7, pl. 1, figs,

3. Bale, 1919; 340. pl. 16. figs. 3, 4,

Shepherd & Watson, 1970: 143,

Records: R, 25-45 m, on Carpopeltic pfiyl-

lopora and Prerocladia licédet.

Muterlaly Luxuriam fertile colonies thickly

oyer-running algae. Stems to 4 mm long.

Sertularia acuta (Stechow,

Colowr—hydrorhiza brown, hydrocaulus bright

yellow,

Remarks: §. maccallumi 15 one of the com-

monest. hydroids in the Pearson J. collection.

Although both species of algae were also

recorded at West L. (Shepherd & Watson 1970),

S. wraccallumi was never Found on P, lucida,

and only occasionally on C. phyllophera at that

locality,

1921), Millard,

1958; 192, fig. 8, Shepherd & Watson,

1970; 140.

Sertularia loculosa Bale, 1884: 9), pl, 4. figs.

5,6; (913: 121, pl. 12, figs. 7, 8; M15: 272.

Tridentata acuta Stechow, 1921; 231.

Sertularia balet Briggs, 1922: 150,

Records; R, 45 my, 8.15 m, on Srenecledia

australis.

Marerial; Abundant fertile colonies, Stems un-

branched, fo 5 mm long, internodes with an

oblique proximal, and a transverse distal joint;

exceplionally, a transverse joint is followed by

2 oblique jomts, Celeyr—yellow. Gonorhecae

with 4-5 deep annulations,

Reinarks: The Pearson 1, specimens correspond

closcly to the short-celled form of “S, loculosa"

Bale.

Millard (1958, p, 198) distinguishes S, acuta

from S, turbinata (Lamouroux, 1816) in her

South African material partly by the presence

of transverse stem nodes in the former species,

and oblique nodes in §. rurpinara. The Pearson

T, material has both transverse and oblique

joints on the one stem, thus further reducing

the difference between these two closely related

species. 8. acuta is a common epiphytic species

in the collection and is associated with only one

specics of alga.

Amphisbetia maplestonei (Bale, 1884), Rees &

Thursficld, 1965; 142. Shepherd & Wat-

son, 1970: 140.

Sertularia maplestone’ Bale,

fie 4, pL 19, fig. 2

Serfularia bidens Bale, |884:70, pL 6. fiz.

19, fiz. 1; 1914a: 14,

Records: R. 34 m; 8, 25 m, among

holdfasts.

Material: Luxuriant fertile colonies.

flexuous, 5-12 em tong.

L884: 70, ph 6,

6, pl.

algal

Stems

Remarks: The distal conical processes of the

gonothecae are modetately well developed, bul

many gonothecae have only 1 process on the

abcauline side.

TY DROIDS (74

Amphishetia pulchella (Thoinpson, 1879).

Shepherd & Watson, 1970: 140.

Serndana palehelia Thompson, 1879: 109, pl

TX, fies, 3, 3a, Bale, 1884: 71, pl. 6, fig. S, pl

19. tig. 10.

Sertularia

1942; 113,

Records; R, 45 m, on Praracladia lucida; §,

14 m, on bryozou epiphytic on algac.

Marerial: A few infertile stems to | cm long,

Remarks: Blackburn (1942) included A. pui-

ehella in the synonymy of A, maplestone? al-

though A. pulchella is a prior numeé. Although

similar in microscopic details of the tropho-

seme, the lwo species seem to be distinct, und

are readily distinguished by the gonothecue and

size of the stem. The stems of A. nwplestere’

ure long and robust, while those of A. pulehella

rarely exceed 2 cm. Both species are epiphytic;

the larger species, A. smaplesronei, is confined

to the hasal parts of algae, while the more deli-

cute A. pulehella epiphytises the fronds. Pos-

sibly, further work may prove the two tu be

ecomarphs of the one apecies.

maplesioned (Bale), Blackburn,

Amphisbetia olseni nsp.

FIGS. 34-37

Type Material and Records; Holotype, NMV

G2001, microslide—R, 33 m, on sponge;

G2097, preserved material, remainder of

holotype colony; paratypes, G2002, G2003,

32004, microslides—R, 33 m. on Herd-

munta moms: G2O0S—S, 17-33 m, on

brown algae, microslide: G2098, temainder

of paratype colony G2003, G2006-—R, 33

m, on red algae, microslide: SAM H34-—R,

33 my, on Sponge. microslide.

Description fram holotype and paratypes:

Hydrorhiza tubular, Stems to 7 mm long,

monosiphonic, stiffly erect, branched. Proximal

stem internodes athecate, terminating in a

strong V-shaped joint. suceecding internodes

thecate, nodes indistinct, but if present. V-

shaped, slender. Internodes 0.52 mm Jong,

diam. at node, 0,06-0,09 mm; 3 hydrothecie

on stem internodes, 1 axillar. 2 subopposite,

Branching regularly alternate, up to S branches

on stem, atising from a long proximal apo-

physis given off at 70° to stem. First branch

internode very short, athecate, with a transverse

proximal, and V-shaped distal joint; remainder

of branch without internodes, but with wp to

5 pairs of hydrothecae. Hydrothecae on

hranches subopposite. in 1 plane, adnate

approx. two-thirds of their lenzth, saccate,

widest near middle. narrowing 2 margin, Fixed

adeauline wall 0.12-0.16 mm long, free nd-

cauline wall 0.05-0.08 mm, standiag our hori.

vontully, of at a slight upward angle from the

internode, Abcauline wall 0,16-0,19 mm, a

pronounced inflextire about one-third the dis-

tance up from the base, followed by 4 sharp

outward bend, but this may be reduced te a

mere concavity in the abcauline wall, Paired

hydrothecae on younger parts of stem and

branches in contact along fixed adcauline wall,

but separated in older parts of stem) if in con-

tuner, the adcauline wall is straight, otherwise

it is bent parallel to the inilexure of the ab-

eauline wall. Margin with 2 long sharply

pointed lateral teeth 0.07 mm long, separated

by a deep, almost horizontal abcauline sinus;

adcauline wall indented behind matgin. Oper-

culum of 2 flaps, abcaulinc component fixed.

Aydranth with approx. 12 tentacles, Gono-

thecae arising from lower stem behind proximal

pair of hydrothecae, large. ovate, fattened,

1,02-1,32 mm tong. Perisare thick, walls

smooth, widening distally to a shoulder 0,84-

1.02 mm width, produced inte a pair of short,

almost laterally directed spines. Aperture citcu-

lu’, 0.35 mm. in diam., with a slightly raised

collar and a ring of minute internal denticles.

Operculum a. circular flap. Gonothecae empty.

Colour—light straw colour,

Remarks; The branching in 4. olseni is regu

larly alternate, where a branch fails to develop,

the stem internode is longer, and has I axillar,

and 2 pairs uf subopposite hydrothecac, then

branching resumes again, The branches are

very brittle and break off eusily wt the slender

proximal joint.

A. olseni 1s closely reluted to both A. prl-

chella (Thompson) and 4, tidens (Bale) in

structure of the trophosume and gonosome, but

is distinguished from these species by the

straighter, Jess flexuous stem, the pronounced

concavity of the abcauline thecal wall, the less

prominent marginal teeth, the greater propor-

tion of the hydrothees adnate to the internode.

and the shape of the gonotheca,

With one exception (8, 17-33 m), the colo-

nies were all found within the same area on the

rough water site.

A_ olseni is named after Mr. A, M, Olsen,

whose interest and encouragement has done

much to foster marine science in South Aus-

tralia.

Amphisbetia minima (Thompson, 1879),

Ralph, !96far 774, fig. & Shepherd &

Wilson, 1970; 140.

FIGS. 37, 38

180

JEANETTE E. WATSON

Figs.

Figs,

Fig.

Fig,

Fig.

wu SO

wus"

38 39 40 4|

31-33. Symplectoscyphus epizoicus n.sp. Fig. 31—Whole stem with gonotheca. Fig. 32 Hy-

drotheca enlarged, anterior view, with hydranth. Fig. 33.——-Hydrotheca, lateral view.

Drawn from holotype,

34-37. Amphisbetia olseni n.sp. Fig. 34.—Whole stem, from holotype. Fig. 35, part of stem and

38.

39,

40,

41,

branch, enlarged. Fig. 36,—Part of stem and gonotheca, from paratype. Fig. 37.—

Hydrotheca, enlarged,

Amphisbetia minima var. pumiloides Bale. Part of stem with two internodes.

Amphisbetia minima var. intermedia Bale. Part of stem with two internodes, Figs. 38

and 39 drawn at same scale for comparison.

Amphishelia minuscula Bale. “Short internode form".

Amphisbetia minuscula Bale. “Long internode” form.

HYDROIDS tat

Sertularia minima Thampson, 1879: 104, pl 17,

fig, 3, Bale, 1882; 21, 45, pl. 12, fig. 25 1884:

$9, pl. 4, figs. 9. 10, pl. 19, figs. 12, 13; 1945;

269; 1924: 248. Mulder & Trefileack, 1914b:

39, Sreehow, 1925. 231, fp. K. Blackburn,

1942: L14. Hadgson, 1950: 23, figs. 41, 42,

Millard, 1957; 221.

Records; KR, 12-50 m;S, 15-25 m, on algae

{see Remarks),

Material) Luxunynt fertile colonies, Stents to

35 mm long. Colow7e—tight brown.

Remarks; Bale recognized 3 varieties of A-

wine jn southern Australian walters, the

largest, var, pumtloides Bale, 1884 (from

Queenscliff, Vic.), a “typical” farm Irom Port

Phillip Bay and New Zealand waters, aud var.

iermtedia Bale, 1915, from the Nuyts Acchi-

pelago in the Great Australian Bicht. Ralph's

(1951) figures und description show her New

Zealand specimens. to be closely allied to the

Australian typical form, but there are nemato-

thecac scattered throughout the hydrocautus, a

condition not normally encountered in the Aus-

Uulian material. 4 minime is one ol the most

abundant hydroids in the Pearson I. collection,

und the material exammed falls with little inter-

vradation into 2 of the varieties, var. pudai-

loides und var. intermedia, Although difficult

to distinguish in preserved material, the vyarie-

hes are casily separated in mounted prepara-

tions. These varieties have not previodsly been

recorded together in the one Jocality.

The present material corresponding to var.

puniufoides is a robust form, conforming to

Bale’s (1884) ceseription. The bydrothecye ure

almost entircly adnate, and the typical wedge

af perisurc belween hydrotheca and internade

is well developed. The gonothecue are variable

in shape, round Lo clongute mm Jatetal view;

those with # raised apertural collar do not have

wring of internal submarginal denticles. The

var. intermedia, not figured hy Bale. as much

smaller, with shorter internodes, and rectilinear

hydrethecae. Nematothecae, varying from

short cylindrical tubules to mere breaks in the

perisarc. are present on all stems, but are cnn-

fned to the infrathecal chamber of the proxi-

faal hydrothecae. Gonothecae sure round [0

ovate, Dimensions of the 2 varieties from

Pearson !. are given for comparison.

var. var.

_ Dimensians. mat pamileides __fatermecia

Internode length 1.35-0,38 A.25-0,37

Digan. al node 0.05-€.08 0.03-0,04

Livdralhecu Tength 24-029 .t7-1.22

With few exceptions (Rilchie I91T), A.

mninwe is recorded as an epiphytic species, and

at Pearson [, the 2 varieties show a stroug

selectivily towards certain species of algae. The

var. puumiloides was found only on the robust

brown aleae Sargassum bracteolosum, 8,

varias, and SY. verrucu/osum, as well as Aero-

carpla puniculeta; var. intermedia Was asso-

ciated with the more delicate red algae Rhoddy-

tnenia australis, Metamasiophera flabellata,

Laurencia elata, and Carpopeltiy phytlophora,

with one record on the delicate brown alga,

Distromium flabellatum. Shepherd & Watson

(1970) noted that many commonly epiphytic

hydroids show varying degrees olf preference

for particular species of algal substrate, but a

differential selectivity by varielies of the same

species has not previously been recognized.

Almost all the colonies have the pegged

hydrorhiza typical of A. minima. Bale (1915)

and Mulder & Trebileock (19I4u) noted this

tact; Ritchie (1931) suggested it muy be a

response 10 Wave action, but Ralph (1961)

could find “no constant relationship vo enyiron-

mental conditions” to accvunt for the thicken-

ings, In many of the colonies of both varieties

of 4. ntinima from Pearson L, the hydrovhtes

is often tubular and loosely winding when in

comuct with the curved and cylindrical sur-

faces of the lower stems of the ulga, then flat-

tening out and developing the transverse murk-

ings as the stolon passes onto (he broader

fronds. This change in cross section of the

stolon may {herefore be etther a response to the

greater movement of the algal frond in turbu-

lent walter, or it may be related to the narure

of the algal surface.

The systematic status of the 3 so-called varie-

ties of A. minima, and of the whole “A.

minha? group, including 4. avniscala Bale,

A. fureaie Trask, and A. stuellevi? Bale, needs

further clucidation. Tt is possible that all may

be ecologic variants of the one species, or

several distinct. bur closely reluted species.

Amphisbetia minuscula (Bale, 1919),

FIGS, 40, 41

Sertifarla minima var. tebathere Mulder &

Trebileuck, 1934b: 40, pl. 4. fig 1-

sSeesatarte puisifla Bale, 1915: 271, pl. 46, figs.

Sertifaria minuscila Bale,

burn, 1942; 114,

Records: R, 30-40 m, on Lauvrencia elite,

Disttomiun flabellaiuin, aod Herdmeania

moms: S, 25-31) m.ion the stem of Cauuvlerpa

sp.. and Halicernaria longirostriy.

Morera; Abiadant colonies, some fertile,

Stemy simple, to 5 min) long, internodes vari-

able. The slems ace divisible into 2 groups—ag

1919; 340, Bliack-

182

long internode group, internodes 1),42—0.44 mm

long, anu « short internode group, internodes

0.30-0,.34 mm long. Nodes of both stem groups

0.06 nim wide, indistinct, transverse, occa-

sionally a V-shaped joint in distal region of

stem. Hvedrethecae similar to deseriptiens al

authors, fixed adcauline wall 0.19-0,22 mm,

free adcauline wall G.07-0,11 mm; abcauline

wall 0.19-().26 mm; an indistinct downwardly

curved ridge passing back from the embayment

between the marginal teeth into the junction of

the adcauline wall with the internode. Gono-

thecae 1.20-1.26 mm long, excluding pedicel,

maximum width, 0.75-0.97 mm, present only

on the “short internode” form.

Remarks; The hydrothecae of the “long inter-

node” form of the Pearson I. material are larger

than those of the “shart mternode” form, but

both ate smaller thun measurements from

microslides of 4. miinuscula, and the type of

“4 minima var. tubathece” in the collection of

the NMY. The “long internode” form conforms

with measurements ot A. pusilla (Bale), while

the “short internode” form is similar to the

var. tubatheca of Mulder & Trebilcock. ‘The

nemitothecue noted by Bale and Mulder &

Trebileock are present in only a few of the

proximal sium internodes of the Pearson I.

specimens; the intrathecal ridge, noted it the

present material, is not present in the type. A.

nunascula displays a wide choice of substrate,

Some correlation evidently exisis between stem

type and environmental conditions, since the

“long. internode” form was abundant on the

sheltered site, whereas the more robust “short

internode” form was found only on the rough-

water side of the island. This suggests that deve-

lopment of a thickened stem with short intet-

nodes is advantageous to withstand rough water

conditions. :

Family PLUMULARILDAE

Pycnotheca producta (Bale, 1882),

Plumularia praducta Bale, |882; 34%, pl. TS,

fig. 3; 1884: 133, pl, (0, fig. 4; 1894; FTI.

Kirehenpuueria prodicta Bale, 1914a; 59, 1915;

302. Blackburn, 1942: 107.

Records: R, 24 m. on Distromitin flubetla-

wm; 8, 24 m, on Avmenera?,

Material A few scuttered infertile colunies.

Stemy to F mim lovg.

Remarks: The material contorms exactly tu

Bale’s description of P. prodnete.

Antennecila tubulosa (Bale, | 894),

FIG. 42

Piganiasia tihalesa Bale,

hes. 2-5,

1894: 114, pl 5,

JEANETTE FE. WATSON

Records: R, 27-30 m, on bryozoa: S, 26-30)

m, On Sargassum sp.

Material: Seyeral colonics, cach comprising a

tew infertile stems, Stems to 3 mm lone, ansing

from a thick hydrorhiza. First internode with

a proximal constriction, fllowed by an athe-

cate Internode with 1-2 nematothecac and an

oblique distal node. Athecate internodes 0,1 1—

0.16 mm long; thecate internodes as described

by Bale, 0.27-0.37 mm Jony, with 1 median

nematotheca and 2 scoop-shaped lateral nenia-

tothecae, Aydrothecae long, 5-G on a stem,

proximal part tubular, perisarc thick, adcauline

wall 0.25-0.27 mm long; abcauline wall 6,22—

0.30 mm long. distal part of adcauline wall

more convex than abcauline side, Margin 0,13-

0.15 mm in diam., deeply sinuated, curving up

to meet produced adcauline wall. Co/our—

yellow.

Remarks: The Pearson L maternal, althougl

definitely reterable to 4, rubrilose, nevertheless

shows considerable variabilicy in thickness of

perisarc, length, diam, af inlernove, and shape

of hydrothecae. Bale (1894) comsidered that

ef, tebdlosa may be a variant of A. canipannla,

or jhe “Antennella” form of an unknown Plu-

mularian,

As the present matenal shows no sitn of

branching, 4. tubulosa may therefore be con-

ssdered 4 distinct spectes.

This is the second record of 4. rebudosa, anc

a first record for S, Aust. (Other locality—Pon

Phillip Bay, Vic.)

Antennella campanuliformis (Mulder & Trebit-

cock, 1909),

FIGS. 43, 44

Pienvlocia campanatiformly Mulder & Trebil-

cock, 1909F FL, pl. T, figs. 6, 9, 10; T9LT: 115.

Records; R. 30-45 m, on Sargassien sp.

Lenvrencta elate and Preroelacie lucida.

Material: Colonies common, fertile, The spéci-

mens contorm to the type microslide of Pfi-

mularia campanuliformis in the collection of

the NMY. The following description supple-

ments that of Mulder & Trebileock,

Hyvdrorhiza tabular. Stems to. 1 cm long, first

stem internode 0.5 mm long, athevale, with 1-2

hematothecae and 1-2 proximal annulations,

distal node oblique, following internodes qlter-

nately thecate and athecate. Thecate internodes

0.39-0.45 m Jong, almost entirely oceupied by

the hydrotheca, with an oblique proximal node,

and a transverse distal node, 0.06-0.09 mm

wide. often indistinct; athecate internode short,

O.2R8-0.31 mm (measured along base of hydra-

HYDROIDS 183

cladium). Hydrarhecae cup-shaped, deep, base

curved, abcauline wall 0.20-0.22 mm tong,

concave: adcauline wall 0.21-41.25 mm long,

straight or wath » slight convexity below the

margin, both walls thickened, the abcauline

flange eXtending back tu the median nemato-

theca, Margin circular, 0.21-0.23 mm in diam.,

slightly »sinuated, Nemetorhecae large, bithala-

mic, O.08-0.L0 mm Jong, distal cup 0.05 mm

in diam, 3 on the athecate internode—]

median, base stout, cup excavated on adcauline

side. 2 laterals below bydrotheca on a very

shart apophysis of the hydrocladium, cups nur-

row. txcuvated on inner side, sides slightly in-

rolled; | on athecate internode, similar ta

other's; 2 similar in shape. but larger than

cuuline nematothecae on the pedicel of Female

gonotheca, facing outwards, cups excavated on

the side facing gonotheca; 1 nematotheca on

male gonotheca above pedicel. Gonothetae of

both sexes on the one stem, arising beside the

median nematotheca on theeute internodes.

male small, 0.22-0.27 mm long, ovate. 0,10-

0.14 mm wide, only on proximal stem inter-

nodes; female large, 0,64-0,66 mm in diam.

globular, only on distal internodes; female

gonophore of | large egg surrounded by a top-

shaped blastostyle.

Remarks: Although Mulder & Trehileock des-

eribe and figure the hydrotheca of 4. campo-

nutiformis as campanulate, this is somewhat

misleading, as the type specimens as well as the

Pearson [, material have almost tubular hydro-

thecae.

This is the second record of A. canrpmiuli-

fermis, and a first record for S. Aust. (Other

locality—Vic_}

Antennella secundaria (Gmelin) s. sp. dubia-

formis (Mulder & Trehbiloock, 1910),

FIGS. 45, 46

Plumelaria debiaformis Mulder & Trebiloock,

1910: 119, pl. 2. fig, 7.

Anrennelfa secuytidarin (Gnielin). Billard, 1913:

Plamularia stcundarja (Gmelin), Blackburn,

938; 346),

Sehizetriche secundaria (Gmelin), Blackburn,

1942: 108.

Records: §, 17-27 m, on compound ascidian.

Rhodymenia austrulis, Distramiam flabella-

tam, Sertuluria unguiculara and sponge.

Material; Abundant fertile colonies. Mydrarhiza

tubular. Sterns lo 6 mm Tong, perisare delicate.

First stem internode Jong, athecate, with 3

nematothecae and oblique distal joint. inter

nade oceasionally with | branch, Following

internodes allernately theeate amd wthecate,

athecate internodes 0.3 mm Tong, with an in-

distinct transverse and a strong oblique distal

joint: thecate internodes shghtly longer, 0.30—

0.35 mm long. Hydrothecae campanulate,

0,20.-0.22 mm deep, set an un angle of 45° to

hydrecladial axis, base flat, abcauline wall

slightly thickened, udeyuline wall almost

entirely adnate, free part closcly adpressed to

internode. Avarefm entire, delicate, 0,26-(,30

mim in diam. Nematothecae as described for 4.

secundaria, 2 present on uthecate internode.

One small suprathecal nematotheca usually, but

not always present in the sinus above the hydro-

theca. Genothecae—male and female on the

same stem, arising beside the median subhydro-

thecal nematotheca, tapering (o a short pedicel.

Female globular, flattened, 0.52-0 58 mm long,

widest. near niiddle. 0.40-0.44 mm maximum

width. cloycd by a thin operculum: 3 nemato-

thecne similar to laterals, in hasal region. Male

gonotheea small, 0.15-0.20 mm long, 0.12-

0.13 mm wide, with 1 proximal nematotheca,

Remarks: The present specimens are identical

with 2 microslides of [tagmentary infertile ma-

teal of Plamularia dubiaformis Mulder &

Trebilcock if whe collection of the NMV.

Mulder & Trebilcock. because of poor material,

were unuble to establish the presence or ab-

sence of the supratheeal nematothecae in P.

dudiaformiy. These nematothecac are clearly

visible in the Pearson [. material-

T have also compared the present material

with fertile material of A. secundaria trom

Mossel Bay; South Africa. provided by Dr

N. A. H. Millard, and with (he exception of the

2 median nematothecac on the athecate inter.

node in the Pearson |, specimens (f in the

South African material). the twa are indistin-

guishuble. As the number of nematothecae on

the athccate internode is not a reliable specific

clitetion, 1 agree with Billard (1913) and

Blackbur (1938) who suggested PL diubia-

fermiy would prove to be a synonym of A.

secundaria.

As the Known South Australian material of

A, secundaria always has 2 nematothecas on

the athecate internode, compared to 1 in the

typical form, und has now been recorded From

two widely separated localities (Pcarson I and

Vic), it Is here recognived as a subspecies of

A. secundaria,

Halopteris suteata (Lamarck, 1816)

Plurnularia saleata Lamarck, (818: 128. Briggs,

1915: 306, pl, 11, fig, 1. Bale. 1914b> 172. pl.

35, figs. 6, 7; 1915: 296.

Plumuteria agliaphenoldes Baie, 1884: 126, pl,

10, fiz. 6.

1x4 JEANETTE

Reeordy; Ro 30m, on sandy floor of cavern.

Material: Several large Fertile colonies. Sten

fuscicled, branched, co 20 em high, growing

from a small fibrous rootstock. Colour-—dtatk

brown.

Reimarks: This species is cusily recognizable thy

its large, erect woody stem, colour, and brittle

texture. At Pearson 1., A. syleata was found

only on the floors of caverns shellored from

gtirse: tL hus however also been noted in open

water to the east, in Tnvestigator Strait (J.W.,

unpublished) at depths of 40 m,

Hulopteris campanula var. campanula (Busk,

1852). Ralph, 1961 6;47,

Plurnelaria carmponita Busk, 1852; 401. Bale,

(884: 124. pl. 10. fig. 5: ISEB: 776; 19t3: 134;

(475; 245, Hodgson, 1950: 40. fiz. 49.

Schizoricha canmpannla (Busk), Blackburn,

1942: 107,

Reeords: KR, 35 m, epilithic,

Murerial; One infertile calony growing from a

common rootstock, Stems —polysiphonic,

branched, to 4,5 ¢m high; some secondary

branching. C'olouwr—yellow.

Renunrks: The specimens agree with descrip-

lions of # canzpanule, and A. campanula vat.

contpunita oF Ralph (1961b)..

Halopteris buski (Bale, (884),

Plamularia bushi Bale, 18845 125, pl. (0, fia.

3. pl. U4. figs, 34. 35; 19)4dur 28, 1915: 296.

Arives, 1915: 304. Hodgson, 1950: 45, fix. 75.

Sehizetricha buski (Bale), Blackburn, 942:

107,

Recardy' RR, 30-338m, on Herdinania

monies, bryozoa and sponge: Stn. F. 65 m.

on werm tube,

Mareriul: Scattered voloniex, euch of iu few

stems ta 2 em long. One stem with immature

inale gonophores

Remarks: The Pearson 1 specimens do not

aliffer significantly from descriptions of [Bile

and Briggs. With one exception (Sin. F) the

colonies are all from the exposed side of ihe

island. They are short and robust. with deeply

incised stem joints; frequently an extra oblique

septal Internodal ridge is developed just below

the adcauline hydrothecal wall, The stems from

less turbulent deeper water (Stn. F) are more

fiexuous, wilh indistinct cauline nodes, and alsu

lack the oblique hydrocladial septa present in

the shallower water specimens. The deeper

water stems were scarlet in colour, Whereas the

shallower water specimens varied from orange

to yellow,

E. WATSON

Halopteris vupposita (Mulder & Trebileock,

1911).

FIG. 47

Plimtlatia appesita Milder & Trebilenck-

1911; 120, pl 2, fig. 5,

Thevoedilus oppositus (M. & T,). Blackbilin,

1938s 316, fig, 2) M42; 17.

Recardy: S, 30 m, on Sargassum spinuli-

gerne and 8. verruculostini.

Mererial: Scattered infertile stems to 12 mm

long, The specimens compare with the type

microslide of Mf. eppeyifa in the collection of

the NMV, and allow a fuller description to sup-

plement the previous brief description of

Mulder & Trebilcock,

Stemy with 2-3 indistinct proximal annula-

tions, followed by a long athecate internode

with 2-3 nematothecae, then alternate thecate

and vathecate internodes of approx, the sarne

length, 0.27-0.39 mm, athecate internades with

a proximal transverse joint and strongly oblique

distal hinge-joint, and 2-3 nematothecuc, if 2,

they ate ane shove the other: the third, if

present, is beside the distal nemalotheci.

Hydrocladia opposite. arising behind the

cauline hydrothecac in middie of the anter-

node, hydrocladia beginning with 2 short athe-

cate internodes, the firs. internode the shorter,

0.95=0,.07 mm long, the second 0.07-0.98 mm

long, with a transverse proximal, and an

oblique distal joint, and occasionally, | nema-

totheca. Thecate hydrocladial internades sinii-

lar ta stem internode. Hydrothecae campinu-

late. 2-3 on hydrocladium, 0.15-0.18 mm

deep, set at 45° to hydrocladial axis. Murgin

0.19-0,21 mm diam., slightly sinuated, rim

eVveried, with a peak on the abcauline side. Ab-

gauline wall 0,12-0,15 mm long, In some

hydrothecue a sinall transverse fold near hase.

Nematothecae 0,05-0,07 mm long, 2 supra-

thecal un stem internodes, 4 on thecate hydro-

eladial internodes—1l median, stour at base.

distal cup cut away on adcauline side, closels

adpressed to internode; 2 lateral stiprathecal.

with slender pedicels, an an apaphysis af tke

internode, extending above hydrotheca, and 1?

small nemalotheca between laterals at hase of

hydrotheea. Hydranth with 10-16 tentacles,

connected to internode by a small orifice in the

upeurve of the abeauline wall,

Remarky: The stem of the type is thick and

robust, and the athecate siem intemodes ave

cunsiderably shorter than the thecate inter-

nodes, with deeply constricted nades-

The Pearson T, specimens have slender stems,

and internodes of neurly equal length, Black-

42,

47.

. 48-52.

HYDROIDS

0.25mm

WU O

O-lmm

Antennella tubulosa (Bale). Part of stem.

» 43,44. Antennella campanuliformis (Mulder & Trebilcock). Fig. 43.—Part of stem with male

s. 45, 46,

gonophores, Fig. 44——Female gonophore-

Antennella secundaria s.sp. dubiaformis (Mulder & Trebilcock). Fig. 45.—Part of stem

with two hydrothecae, Fig. 46—Empty female gonotheca.

Halopteris opposita (Mulder & Trebilcock). Hydrocladium with one hydrotheca.

Gattya trebileocki n.sp. From holotype. Fig. 48—Whole stem. Fig, 49.—Hydrocladium

with three hydrothecae. Fig. 50.—Hydrotheca, anterior view. Fig. 51.—Twin lateral

nematothecae from distal end of hydrocladium, enlarged. Fig, 52,.—Median nematotheca

on thecate internode, enlarged.

hum (1938) also noted this feature in his mute-

ful Erom the Sit Josenh Bunks Group, and pon.

sidered that it may “constitute a distinct

variety”. As the type microslide consists of a

single sten) fragment 3 mm long, il scems pos-

sible that the Sevth Australian maternal nay

better represent The species than the type it-

self.

This is whe third record of Ff. apposita.

(Other localities—central Vic. Sir Joseph

Banks Group, S. Aust.)

Gattya aghovheniaformis (Mulder & Trebil-

cock, 1909),

Plimularia dglaopheniaformis Mulder & ‘Trebil-

cock, 1909: 32, pl. 1, fig. 7

Hafonteris agliapheniuformis (M, & T.), Shep-

herd & Watson, 1970: 140,

Records: R, 18-33, on Phurtuiuria procum-

bens and Callophiyllix coecined,

Muterial: Several colonies of a few infertile

stems each. Mydrorhiza tubular. Scenis to'7 mm

long, bevinning with an athecate internode with

1~3 pairs of couline nematothecae: thecate

internodes. with a proximal hydrotheca, and 2

pairs of suprathecal nematothecac. Hydroctadia

arising from a small apophysis behind hydro-

thee», the first pair opposite, first 2 hydrocladial

internodes slender, short, athecate, 0.04—-0,06

mm long, with transverse joints. distal internode

longer. 0.07-0.09 mm, with 1 medinn nemato-

theea. Mydratheeae 0.17-0.20 mm deep (fateral

view), with broadly lobed margin 0.13-0,18

mm in diam, the anterior and posterior lateral

projections curving inwards Over the aperture,

Remarks: The marginal projections of the

Pearson [, specimens. differ from those of P.

ughophentaformis fiznured hy Mulder & Trebil-

cock. Furthermore, the cauline internodes are

vuriable in Jength, some heing barely long

enough to accommodate the hydrotheca; those

Stems with longer internodes also have a thin

perisarc, are more Hexwous, and have a less

deeply lohed hydrothceal margin Uhan the type.

Following Millard (1962, p. 270), this and

nther species with a toothed thecal margin are

referred to Gatrya,

Gattya balei (Bortlett, 1907).

Plamularia bealei Bartlett, 1907+ 65, Mulder &

Trebileack, 1909; 29, pl. 1, fizs. I-39. Hale:

1919: 344, pl. 17, fig. 6.

Records; R, 14-45 mt on Metamastophara

flabellata, Pterocladia lucida and Ptere-

siphonia?.

Afatertal: Colonies conimon. A few fertile stems

with female gonophores, Sténes te 7 mm long.

JEANETTE E. WATSON

Cojaur—vellow,

Remarks: This rare but distinctive species has

not been recorded previously in S. Aust. (Other

locality—eentra] Vic.)

Gattya trebileocki sp,

FIGS. 48-52.

Tepe Matetlal and Records: Holotype. NMV

(52029, microslide, G2099. preserved mate-

tial, remainder of holotype culony=-R, 10—

33) m, on fragment of Caulerpa brewnil-

paratypes, G2030, G2037, G2032, G2053,

G2034. G2035; SAM H39, microslides—R.

10-33 m, Gn Caulerpa brownit; G2100, pre-

served material, remuinder of paratype colo-

nies,

Description from holorype and paratypes:

Uydrorhiza tubular, of same diam, as stem,

embedded In the stem of the alga, Sreaw to $

mm long, proximal stem intertrode 0.70-0.75

mm long, athecate, perisare thick, with a few

rough annulac constrictions, and 1-2 distal

nematothecue: distal hinge joint V-shaped, Fol-

lowing stem internodes alternately thecale and

athecite, thecale internodes 0.25-0.45 mm

long, athecate internodes 0,10--0.13 mm long.

average diam. of internode 0.10 mm. Hydro-

cladia arising From a short apophysis of the

stem above the bydrotheca on euch cauline

interrode, first pair opposite, following hydro-

cladia altecnate. Hydrocladium with 1-3 hyudra-

thecac, thecate and athecale internodes alter-

nate, crowded. identical to cauline internodes.

Athceate internodes very short. 0.04-0.06 mm

long. 2 between hydrocladial apophysis and

first thecate internode, distal joint oblique, the

second internode with oblique distal node. and

{ median pematotheca; following internodes

alternately alhecate and thecate, athecate inter-

nodes 0.07-0.08 mm long, thecate internodes

21-029 mm long, with oblique proximal and

transverse distal nodes, Ilycrothecue distal on

internode, cup-shaped, U.t4-0.20 mm deep,

perisare delicate. base curved, set well Jown

in hydracladtum; abeauline wall 0.15-0.20 ram

long, convex, thickened to hase of median

nematotheca: adcauline wall shorter, 0.12-0,17

min tong (to end of lobes) not thickened.

almost straight, Afargin sinuated. (20-0.25

mm in diam., with 5 lobes of which 3 wre well

developed, tongue-shaped—1 unterior. peaked.

tising over aperture. 2 posterior, paired, with a

deep sinus between, and 2, paired. in middle of

margin, broad and low in lateral view, hut often

obscure Nemarothecae hithalamic, of 3 types—

1 medion, on each athecate internode (except

HYDROIDS th?

first hydrocladial internode), base slender,

distal cup deep and rather natrow; 4 nemato-

thecae on theeate internodes—! snedian, base

very stout, 0.08-0.10 mm long, distal cup €x-

eavated on adcatiline side, cup 0.04-0,06 mm

im diam,, margin vertical. closely adpressed to

hydrocladium; 2 posterior Jaterals, longer than

medians, 0,08-0.10 mm long, distal cup wide

and shallow, 0,05-0,08 mm in diam., slightly

flattened on adcuuline side, overtopping mar-

ginul lobe of hydrotheca, base slender, on a

pedicel 0,06-0.08 mm long; t small median

suprathecal, similar to nematotheewe on athe-

cale internudes, but smaller, deeply set between

the twin laterals at base of hydrotheca.

Hyedranth with approx. 16 tentacles. Colous—

pale yellaw. Gonotheca absent,

Remarks: G. teebilgocki shows close affinity

with G, aglaopheriaformis Mulder & Trebil-

cock, but may be easily distinguished from, this

species by the shape of the posterior marginal

lohes of the hydrotheca, which in G. trebilcocki

are rounded. The cups of the lateru! nemato-

thecae are also much larger in G. trebilcocki.

Both species occur in the same locality and

over a similar depth range, but G. agiaophe-

niuformisx as presently known is an epizvic spe-

cies, whereas G, trebileock? has been found

only on algal substrate, Both species are Tare.

Pluniularin procumbens Spencer, 1891: £40,

pls. 21-23, figs. 17-25. Bale, 1894: 115,

pl, 5, figs Lt, 125 1914a: 29: 1915: 297,

Briggs, L915: 30S, pl. LO, fig 1,

Records: R, 33 m. epilithic on vertical rock

faces.

Material: One infertile colony 7.5 em high.

Srem thick, fuscicled, growing fram a fibrous

rootstock. Shore hydrocladial internodes with

nematothecue ax described by Bale (19140)

and Briges (1915).

Remarks: Although only 1 specimen was col-

lected, several mature ¢culonies of similar size

and appearance were noted, The colonies arc

amall io comparison with Briggs’ Tasmanian

material and Spencer's material from Port Phil-

lip Bay, Vic. Bale (1914a, 1915) does not give

dimensions of FP. wrocwinbens from the Great

Australian Bight,

Phimularia asymmetrica Bale, 191 4a: 29, pl. 4,

figs. 2, 3; 19152 279,

FIG. 53

Records; Sin. F, 65 m, freegrowing on sandy

bottom

Meresial) (ne infertile colony, 30 ¢m high.

Stem jong, flexuous, branched, strongly {s-

cicled near base. Hydrocladia with 12-15

hydrothecae, hydrocladiai internodes with 5-7

strong septal ridges, Hydretheeae long, adnate,

abcauline wall curving over distally towards

hydrocladium; an indistinct intrathecal fold

sometimes present about halfway aluny thecal

wall. Margin with 2 broad bluntly pointed

jateral Jobes, usually of the same size and

shape, occasionally | lobe much more promi-

nen than the other.

Remarks: The Pearson |. material shows some

variations compared with Bale's microslides uf

-Endeavour’ material from the Great Australian

Bight in the collection of the NMV. The “En-

deavour’ specimens show considerubly more

curvature of the distul hydrothecal abcuuline

wall than the Pearson 1. material, Haye a dis-

lince oblique intrathecal ridge, and a maximum

of 4 septal ridges ia the internode. The mar-

ginal lobes of the ‘Endeavour’ specimens sel-

dom show the pronuunced degree of asym-

meliry inferred from Bale’s figures of P. usyu-

metrica. Furthermore, the margins of the lobes

are reunded, rather than pointed, and each pair

is usually the sante shape; however, as the

hydrathecal margin itself is slightly oblique to

the hydrocladial axis, the lobes appear asym-

metrical when viewed from abeve,

P. asynunetica shows g strong resemblance

to «figures and description of P, Aerrmwipzé

Stechow, 1909 from Japan (Bile I9l4a, p. 31)

and P, #uberert var, elengata Billard, 1913

from the Indo-Pacific revion. The latter is a

small species 2-3 cm high, and the hydracladtal

internodes and hydrothecae appeie to be indis-

inguishable from P. asymmetrica fram Pearson

I, The Jess distinct intrathecal fold and more

symmetrical marginal lobes of (he Pearson I,

specimens tends to bridge the gap between /’.

asymmetrica and Py hertwigi. Possibly all are

geographical variants of the one species.

Although only | colony was collected, the

species was a dominant member of the seafloor

community of the deeper water. Many of the

ulder colonies were almost completely invested

hy wa growth of a pink coloured epizoie zoun-

thid, the weight of which bends the colonies

over to touch the sand,

This is the fourth record of Pi asvanmerrlea;

other records are ulso from the Great Austra,

lian Bight.

Plumularia flexuosa Bale, 1894: 115, pl 5,

fies. 6-10. Mulder & Trehilcock, 1916: 78

{discussiun). Stecbow, 1925: 246. Black-

183

burn, 1938: 315. Shepherd & Watson,

1970: 140.

Pluntalaria pulehella (Bale), ‘Totton, 1930:

221, fig. 58.

Records: R. 27-45 m, on Mvchoden carnosu.

Material: A few infertile stems, Siems to 3 mm

long; internodes Jong, flexuous, nutes tans-

verne, 3 cauline nematothecae on an internode

—?2 uxillar, and 1 proximal, exactly as des-

cribed anu figured by Bale (1894) for P,

(lexuutase,

Reraurks; [ have examined a series of micro-

slides of FP pulchella Bale, 1882, and P,

flexwese in the Bale collection of the NMV.

The stems of P, pulehella are robust, with

several transverse cauline internodal septa, but

have no cuuline nematothecae. Hydrocladia

and hydrothecae are identical in both species.

The yornotheca uf P, putchelle is globular,

with an oblique aperture, and 4 rw of large

internal submarginal weth. In PF. flexuosa, the

gonotheca is clongate, twice as long as wide,

and there are no submarginal teetlr.

Although Bale (1894) clearly distinguished

between the two species, Totton (1930) united

them in P. pufchella on the grounds that “P,

flexaesa . - . appears to fall well withia the

Tange of variation of this species™ «ie. P. pul-

chefla) as the stems of some of his material

were “fine and fcxuous, while others were stout

and straight", His synonymy has since heen

followed by Ralph (1961b) and Millard

(1957).

Stem thickness and the presence or absence

of cavling nematotheeae are frequently un-

reliable specific criteria aniong the Plumu-

Jariinae, but tuking into account the difference

between the gonothecuc (unless sexual dimor-

phism can he demonstrated) it scents best, fol-

fowing Blackhurn (1938), tu regard the two

as distinel species.

Although associvted with a range of algal

substrates in other localities (J.W. unpublished)

P, flexnosa occurred only associated with a

delicate species of the red algal genus My-

chedea (nsually placed under M, carnosa in

herburiu), The growth habit of the trydroid is

unusual and was first poticed by Dr. H. B. S,

Womersley and G, T, Kraft who supplied the

following descciption. “The hydroid infests the

Mychodea frands from «@ very early stage, with

frands less than | cm high showing abundant

hydroid stolohs. The stolons penetrate length-

wise through the outer medulla of the alga.

branching occasionally laterally, and producing

at regular intervals through the cortex the erect,

JEANETTE E. WATSON

polyp-bearing axes. As the Mychodva plant de-

velops.. proliferation of the hydroid stolons in

the lower axis breaks down the algal tissue until

the Mychodey is attached to the substrate only

by a detise weft of hydroid. This may be 2-8

mm thick and a centinetre or more jung, sup-

porting a much branched Mychodea plant over

20 cm long and infested throughout with the

hydroid.”

Plunularis spinuloga Bale, 1882: 42, pl. 15,

fig. 8 I8S84: 139. pl. 12, figs, 11, 12:

1888; 783. Stechow, 1925; 246, Mallard,

1962; 301,

FIGS, 54, 55

Plumidaria spinitese var. spinulosa Ralph,

LY6.: 37, fig, 4. Shepherd & Watson, 1970> 140,

Reeordy: R, 18-30 mm, on Lanrencia elute,

Plecamium angustum, Thyroscyphis mar-

ginatuy and Aglaopitenia plumosu.

Material: Abunctant infertile colonies of 2 few

stems ech. Hydrorhiza wide and flat with

transverse dark markings. Stents to 3 mm long.

intemodes of variable length, 0.17—-0,21 mm,

width at node 0.02-0.04 mm Hydrovladia

arising near middle of short internoues, distally

On long internodes. Hydrothecae 0,16-0.18 mm

deep, abcauline wall strongly convex, Terminal

hydroclaciul spines well developed, varying

from long und sharply pointed to blunt and

barely protruding, past hydrothecal margin,

Netnatathecue identical with typical form, but

pedicels of the median hydrocladial nemate-

thecue show considerable variation in thickness.

Reniarks: The Pearson 1, matertal shows a wide

variation in size of the stem internodes, position

of the hydrocladial apophyses, width of the

hematothecal pedicels and length of the ter-

minal spine. Those hydrotheeae with more pro-

hounced terminal spines arc always larger and

more robust in appearance than those with the

Shorier spines. Because of the variahility of

length of the terminal spine, Millard (1061)

n® longer recognizes the distinction. between the

varicties of P, spintlosa (Le var. pypica

Stechow, 1923 — var. spinulosa Ralph, 1961,

and var. obtusa Stechow, 1923). The present

materi] supports her view.

No correlation was eviden| between stem

type, substrate, or environmental conditions.

Plumularia goldsteini Bale. 14982: AL, pl, 15,

fig. 7: 1884; 157, pl.11, fig, 9,

Records: R. 30 m, on Delisea pitlchra,

Material: A few infertile stems to 3 mm lou

Remiarkiy The specimens conform exsctly to

the description of P. poldstein? by Bale.

HYPROIDS

A new record for $, Ayst. (Other loeality—

Vic.)

Plumularia obliqua (Johnston, 1847), Bale,

I884; 138, pl 12, figs. 1-3, Blackburn,

1942. 108.

ai asad obligna Johnston, 1847; 106, pl. 28,

Records: R, 20 tm, on Melanusiephore fla

bellatn; S, 30 mon Sargassum sp,

Material: A few delicate infertile stems to 4

mm long.

Renwarks; The material conforms to descrip-

lions of PF. oblique hy Bale.

Phonulmia australis Kirchenpaver, 1876. Bale.

I884: 143, pl. 12, figs. 6, 7, pl. 19,, digs.

43, 44.

Plumularia obligue vac. adsirelis Kirchenpauer,

(876: 49, pl. 6, fig, 10,

Reeaus: S$, 14 m, on the seagrass Posidonin

australis.

Material: Luximant infertile colonies, Stems to

4 mm long, srising from a broad fat hydro-

rhiza with transverse dark markings.

Remarks: The Pearson Lo material compares

with Bale’s (1384) description of P. wnsyrelis.

The median nematothecne are, however, not is

deeply exeuvated on the adeauline side nor as

closely adpressed li the bydrocludium as in his

figures. ‘The aaillar monothalamic nemato-

thecat are absent from many stems.

Plumularia epibracteolosa o.sp.

FIGS, 56-60

Type Material and Records: Holotype, NMV

(42046, microslide; G210] preserved mate-

nial, remainder of holotype colony; para-

tvpex, G2047, G2048, G2049, G2050,

G205!; SAM H37, microslides; all material

—R, 50 m, on Sargassum bracteolasye,

Description fren feletype and peralypen:

Aydrorhiza flat, reticular, 0.25 mm wide, with

pegeed borders, radiating from a digitate sto-

lunic plate, Steets monosiphonic, to 2 em long,

perisare thick; proximal internodes toughly un-

dulated, without hydrocladia, nodes indistinct,

following internodes hydrocladiate, 0.36-0.45

min iang, 0.14-1.85 mm in diam., proximal

and distal nodes oblique, V-shaped. Perisarc

smooth externally, internally ridged by 3—+

intemodal sepla—t above, and 1 belaw nore,

1-2 in middle of internode, ridges fewer in

younger parts of stem; either absent or inci-

piently developed in younger stems. Hy«lro-

eludfie alternate, 1 on each slem tnternode, tn

| plane, arising from a shor distal apophysis of

189

the stem, One or two hydrothecae on hydro-

Cladium: hydrocladium beginning with 1, occa-

sionally 2, short proximal athecate internodes

0,09-0,12 mim long, proximal, hode transverse.

distal node slightly oblique; thecale inlernode

0.23-0.27 mm long, socketted into the athecate

internade by a slender joint; hydrocladia below

internode straight, blunt end not projecting be-

yond thecal margin; 4—5 oblique interngdal

sepla dividing internode into segments, 2 below

median nematotheca, sloping opposite ways,

and 2 below the hydrothecu. When 2 hydro-

ibecae are present on hydrecladium, they are

separated by 2 athecale internodes, the first

short, ©.07-0.09 mm long, with transverse

joints, the next 0,12-0.16 mm long, with a

socketted proximal 2nd an oblique distal joint

and Ll median nematotheca; both internodes

without septa. Hydrothecae wide, shallow, cup-

shaped, 0.15-0.17 mm deep, with a Hat base,

set an the 3 strong convexitics of the hydro-

cladium; abcauline wall straight, 0.11-0.13 mm

long, thickened by a continuous flange of peri-

sare extending the entire length of the thecate

imernode; adcauline wall 0.10-0.11 mm tong,

slightly convex, adnate to hydrocladium only

neur base, the remainder joined to the hydro-

cladium by a wedge of perisarc. Margin 0,14—

0.19 mm in diam. (laleral view), sinuated, with

a thickened outwardly rolled rim, the line of

the margin curved down to meet the hydro-

cladium, but the aperture truncated by a deli-

cate transverse shett of pensare extending

across the cup 0.05 mm above adcauline wall.

Neimuothecae all of similar shape and size,

0.06-0.09 mm long, bithalamic, distal cups

shallow, entire, 0.03-0,04 mm in diam.; 2

cauline with slendor bases, 1 in middle of stem

internode, often missing, and 1 axillar; 3 on

thecate hydroclidial internodes—i, median,

hase stout, cup slightly excavated on adcauline

side, 2 laterals below the hydrotheca, bases

stout, cups narrow, standing upright on hydro-

cladium but not reaching top of transverse peri-

sarcal web, One minute mamilliform pore pre-

sent on the shoulder of the hydracladial apo-

physis. Aydranth with approx, 24 tentacles.

Gonothecue large, 1-2 on lower stem on

a short pedicel arising from an old hydroela-

dial apophysis, elongate oval, 138-18 mm

long (including pedicel} maximum diam. 0.72—

1.02 mm (at two-thirds the distance up from

pedicel) perisare delicate, smooth, or slightly

uncdulated, no operculum, top closed hy a thin

convex membrane. Gonophores male, mature.

surrounded by a thin blastestyle Celaur—

stems bright yellow, gonothecac orange.

19%) JEANETTE E. WATSON

Fig, 53.

Figs. 54,55. Plumularia spinulosa Bale. Fig, 54.—Part of a stem with larger hydrothecae and prom-

inent terminal spines. Fig. 55,—Stem wiih smaller hydrothecae and blunt spines.

Figs.. 56-60. Plurwlaria epibracteolosa n.sp, Fig,

ot stem showing internadal septa a

Plumularia asymmeirica Bale. Part of hydrocladium with two hydrothecae,

56.— Whole stem with stolonic plate. Fig. 57.—Part

nd cauline nematothecae. Fig. 58.—Hydrocladium

with two hydrothecae. Fig. 39.—Hydrotheca, dorsal view. (Figs. 46-59 drawn from holo-

type). Fig. 60.—Group of two male gonophores, fram paratype,

Remarks: P. epibracteoloxa is closely allied to

the P. setaceoides group endemic to Australia

and New Zealand, It shows some affinities with

P. excavata Mulder & Trebileock, and with P.

corrugatissma Mulder & Trebilcack, bug is

easily distinguished from both these species by

the structure of the hydrothees and from P.

corrugatissma by its greater overall size.

Stolonic reproduction, common among some

species of the Plumulariinae, has been discussed

by Billard (1904) and Gravier (1971) but has

not previously been reported among the Aus-

tralian members of the subfamily. Many stems

of P. epibracteclosa show various stages of dis-

tal enlongation into a tendril which flattens out

laterally into an embryonic stolonic plate. This

plate adheres to the edge of a nearby algal

frond, sending out hydrorhizal filaments to

form a new colony, the parent stem ‘finally

breaking away. [n one case (holotype imicro-

Slide) # stem has re-attached itself by the dis-

tal end to the same stolonic plate, forming a

closed Inup.

P. epibracteolosa exhibits extreme variation

in development of the cauline internodal septa.

The older stems, distinguished by the thicker

perisarc, are heavily internally ridged, while

the younger stems have either none at all or

show a gradational development between the

two extremes. The presence of internodal septa

has often been accepted as a diagnostic charac-

ter within the Plumulariinae, but the variability

of P. epibracteclasa demonstrates the un-

reliability of this criterion,

HYDROIDS 191

The fronds of the substrate alga Sergusrsune

bracteolosum are seasonal, growing fram Sep-

tember to February (Shepherd & Womersley

1970), P. epibracteolasa must therefore spread

very rapidly in order to form fertile colonies

within a very shurt period. This may account

for the unusual propagation of the colonies by

both normal growth and stolonic reproduction.

the fatter method ensuring spread of the

calonics from one part of an alga to another.

Although the alga, §. bracteoloswn, is also

very common at West I, (Shepherd & Womers-

ley 1970), P. eplbracteolosa Was never recorded

from this locality. At Pearson 1, the alga was

restricted ta a: Jimestoie seafloor in moderate

surge at a depth of 50 m, at a distance of 400

m offshore. The colonies of P. epidracrealesa

accur only on the fronds, whereas Amphixbesia

mlninwe var. pumileides Bale exclusively

epiphytises the harder stems of the alga.

Momolaria meretricit o.sp.

FIGS, 61-64

Type Material and Records: Holotype, NMV

G2n55, microslide; G2102, preserved

material, remainder of holotype colony—

R, 27-30 m, on sponge on vertical walls;

paratvpes, G2054, G2055, G2056, G2057,

G2058, G2059, SAM H38, microstides;

G2103, G2104, preserved material, remain-

der of paratype colonies—S, 18 m, on

sponge on tuck walls,

Description fram jelotvpe and paratypes:

Aydrarhiza tubular. Stems monosiphonic, erect,

straight, to 1S mm long; stem internades 0.42--

0.51 mm long, smooth, the proximal internode

beginning with a transverse joint near hase of

stem, following intemodes with an oblique

proximal joint, often indistinct, and a strong

distal joint, 0.06-0.09 mm in diam. Aydre-

cladie alternate, 1 on each internode, widely

spaced, arising from a distal apophysis 0.05

inm fong. and 0,08 mm in diam, at extremity

of internode, with 1, occasjonally 2 hvdro-

thecve, and rarely, a secondary branch given

Off behind the first hydrotheea, Hydrocladium

with either L long smooth proximal athecate

internode 7.14-0.19 mm long, and 0.07 mm

in diam., of alternatively, 2-3 short athecate

internodes 0,05-0.12 mm long. with internally

Tidged perisarc, These are followed by a long

thecate internode 0.30 mm long, entitely occu-

pied by hydrotheca and an infrathecal cham-

ber 0.10 mm Jong, terminating behind hydro-

thecal margin, Mydrorhecee campanulate, O15

mm deep, at 40" to hydrocladial axis; alcauline

wall rounded in lateral view, almost entirely ad-

nate and immersed in internode, abcauline wall

straight, expanding, contiguous with Iine of

upper wall of hydrocladium, very slightly con-

stricled behind margin. Murgin evérted, 0,18

mm in diam., slightly simuated, curving dows

und back to adcauline wall. Nemutothecae

bithalmic with slender bases and shallow distal

cups partially cut away on the abcauline side,

occasionally 1-2 halfway up stem internode an

opposite side ta hydrocladium, and 1 axillar, 3

present on thecate internode—! median, 0.04-

0,06 mm long. adpressed to the intrathecal

chamber, and 2 laterals below hydrotheca,

0.03-0.04 mm long, distal cup entire. One

very prominent monothalamic mamilliform

pore, with 1, sometimes 2 orifices on short

tubular necks projecting from the top of the

stem apophysis, Gonotleca absent.

Remarks: P. meretricia, like P. epibracteclosa;

shows considerable variability of features

usually regarded as reliable specific criteria

among the Plumulariinae, The younger stems

have a smooth glassy appeurance, with long

stem and hydrocladial internodes, and also have

cauline nemutothecac, The stems seldom retain

their chuline nematothecsac after maturity,

showing only scars where the nematothecae

have dropped off, Since many of the younger

siems show neither scars nor nematothecae,

and in some cases, the axillar nematothecae

have failed to develop as well, the presence or

ubsence of these structures cannot be regarded

as diagnostic of the species, The mamilliform

pore is however, a constant feature of all the

stems, The regenerated athecate hydrocladial

internodes common in some stems, mark the

site of repeated hrenkage and regrowth of the

hydrocladium. In these cases, a short athecate

internode is first added, follawed by an em-

bryenic hydrotheca and infrathecal chamber.

Nematothecue bud off Tater as the hydrotheca

nears maturity. The athecate intemode at this

stage is without internal perisarcal ridges. These

develop ag the lrydrocladium ages.

P. meretricia shows some relationship with

P. flexuosa Bale and P. hyalina Bale, but it ts

much larger and more robust than cither of

these species.

Phimalaria togata o.sp.

FIGS 65-67

Type Material and Records: Holotype, NMV

G2060, microslide—R, 33 m, on Metavonin-

lithen eharoides: paratypes. G2061, G2062,

G2063, G2064, G2065, G2n6, SAM Ha4fi,

192 JEANETTE E. WATSON

WW OZ

wuo-|

0.25mm

Figs. 61-64. Plamularia meretricia n.sp. From holotype. Fig. 61—Whole stem, Fig. 62.—Part of stem

with young hydrocladium and smooth athecate internode, Fig, 63.—Older hydrocladinm

with regenerated athecate internodes. Fig. 64.—Mamilliform axillar namatotheca, en-

larged.

Figs, 65-67, Phumiduria togata n.sp, From holotype. Fig. 65.—Part of stem. Fig. 66—Hydracladium

and hydrotheca,. lateral view. Fig. 67-—Hydrotheca, anterior view, showing aperture.

microslides, C2105 preserved material, re-

mainder of paratype colonies—S, 30 m, on

Meteagonialithan charaides.

Description from holotype and paratypes:

Hydrorhiza broad and flat with transverse dark

markings. Stems short, to 4 mm long, mono-

siphonic, flexuous; 1-3 short proximal inter-

nodes with transverse nodes, following inter-

nodes hydrocladiate, longer, 0,03 mm long,

0.08 mm maximum diam., smooth, proximal

node transverse, distal node V-shaped, a strong

transverse septum above the node. Hydrocladta

short, alternate, 1 on each internode, arising

from a distal apophysis, with 1 very short

proximal athecate internode 0,03-0,04 mm

long, followed by a longer athecate internode

0,19-0,21 mm long, curving very slightly below

base of hydrotheca. Hydrothecae subglobular,

0.20-0.22. mm. high from base to crest (lateral

view). 0,16-0.18 mm wide (front view). ab-

cauline wall rising perpendicular to hydro-

cladial axis, then curving over and hack to

thecal margin; adcauline wall rounded, set well

into hydrocladium, free part rising in a sinuous

curve to the margin. Infrathecal chamber 0,1 1—

0.13 mm long, maximum width 0.10-0.12 mm.

the proximal joimt slenderly pointed and

socketted into the athecate internode. Nernato-

thecae bithalamic, with slender bases, terminal

cups wide, a little cut away on adcauline side:

2 cauline—1 axillar, 0.07 mm long, and 1,

same as axillar, one third distance up internode,

on opposite side to hydracladium; 3 bydro-

cladial nematothecae, 1 median, 0.05 mm tong,

HYDROIDS

adpressed to. the infrathecal chamber. 2, slightly

smaller, standing upright on a projection of the

hydrocladium below hydrotheca, barely reach-

ing thecal mirzin, and separated at the base by

a Tounded prominence. of the hydrocladium.

Gonotheea absent.

Remarks: P. jegata is a very small species

closely allied to P, fivalixe Bale, from which it

may be distinguished by its smaller size, the 2

cauline nematothecac, greater curvature of the

abeauline hydrothecal wall and the distinctively

hooded appearance of the margin.

Plamolaria australiensis o.sp.

FIGS. 6871

Type Materia? and Records: Holotype, NMV

G2067, microslide, G26 preserved mat-

erial, remainder of holotype colony—R. 20-

25 m on sponge: paratypes. G2068, G2N69,

G2070, G2071, SAM H41, microslides—R.

20-25 m, on sponge.

Wescrintian from holotype and paratypes:

Hydrorhiza tubular, embedded in surface of

sponge. Siem monosiphenic, flexuous, to 15

mm long, petisare thick, occasionally heavily

thickened at point of regeneration of a new

atem from the broken butt of an old stem,

Internodes variable in length, G.06—1.5 mm,

nodes transverse, distinct, width at node 0.)4—

0.25 mm. proximal 24 internodes withour

hydrocladia, Internodes with 6-12 cauline

nematothecve scattered in 2 vertical rows in the

same plane as hydrocladias axillar nemuto-

thecac absent, hut 7 nematotheca usually

present on intetnode just above hydrocladial

apophysis; older internodes with fewer nemato-

thecae. Hydraciadiq to 2 mm long, alternate

to subopposite (exceptionally. lower hydro-

cladia may be opposite} directed upwards in 1

plane from a short apophysis of the stem: 1—3

hydrocladia on internode. arising near Lop,

middle. or hase of interaode, but this is

variable; shorier internodes have fewer hydru-

cladia. Hydrocladial internodes alternately

athecate and thecate, the proximal athecate in-

ternode with 1, occasionally 2 nemutothecae:

following athecate internodes 0.27-0,32 mm

long (measured along base of hydrocladium)

with a transverse proximal, and strongly

oblique distul joint, and 2 nemaflothecie.

Thecale internodes 0.18-0.20 mm long. 0.06-

0.08 mm in diam. at transverse (distal) node,

4 maximum of 7 thecate internodes on a hydro-

cladiuim, and frequently, 2 transverse intermodal

septum below pedicel of lateral nematotheca.

Thecate Internude with 4° nematolhecue—!

Tus

median, subhydrothecal, 2 lateral, and | supra-

thecal. Alydrathecae asymmetrical in lateral

view, wider than. deep, scoop-shapéd, set al

abvut 45° to the hydrocladial axis, abcauline

wall straight or very slightly concave and a iitle

thickened, 0,16-0.20 mm long; adcauline wall

convex, 0.13-0.19 mm long, the shallow curve

of the wall contiguous with the base of the

hydrotheca. Margin 0.25-0.3L mm in diam.,

entire, delicate, at an angle of 30° to the hy-

drocladial axis. Nematorhecee bithalamic, all of

similar shape and size. the cauline nemnatothecse

with moderately slender bases, cups shallow,

adcauline wall excavated; 2 median. nemato-

thecae on athecate mlemode, similar to cauline

nemiatothecae, O.07-0.08 mm long, bur with

more robust bases, closely sdpressed to inter-

node, the proximal nemutothecae frequently

somewhat smaller than the distal. Theeate tnter-

node with 1 median subhydrothecal nemato-

theca, cup deeply excavated, pressed close to

base of thecal wall; 2 taterals with shallow open

cups 0.05-0.06 mm in diam... slighthy cnt away

on udcauline side, the edge of cup not reaching

thecal margin, base slender, seated on a pedicel

0.05-0.06 mm long, arising at the junction of

the adcauline wail with internode; 1 small leaf

shaped monothalamic suprathecal nematotheca,

set deep in sinus behind hydrotheca, the aper-

ture facing inwards, Gorothecaa present, male

and female urising beside median subhydre-

thecal nematotheca, usually tn proximal region

of hydrocladium, sexes usually separate, occa-

sionally both sexes present on same hydro-

chidiam. Female gonotheca pear shaped, 0.18-

0.25 mm long {excluding pedicel) 0.42-0,55

mint maximum width, with 1-2 nematothecae

in the basal region similar to the laterals, but

lurger. Operculum a thin flap of same size a5

top of gonotheca. Male gonotheca smaller than

fernale, slipper-shaped, 0,13-0.16 mm wide,

with 1 proximal nematetheca, a little smaller

than those on female ponotheca. No uper-

culum, Pedicel a small round seginent 0.07 mm

in diam, in both sexes,

Remarks, P. catitraliensis is closely related to

P. bedoti Billard from the Indo-pacific and P-.

westnt Jarvis from South and Last Africa, but

is distinguished from both these species hy the

shallow scoop-shaped hydrothecae. It also

shows some affinities with some Indo-Pacific

members of the genus Halepteris, ea. H. buski

(Balc) (a deeper water species common on the

sOuthern Australian constline, alsa found at

Pearson 1.}. and with A. polymorpha (Billard)

in size gnd shape of the gonothetse and nema-

194 JEANEITE

tothecae, general aspect of the colonies, and

the tendency toward opposite branching in the

hasal stem region,

Aglaonhenia plumosa Bale, 1882: 37, pl. 14.

fig. 6; 1884: 153, pl. 14, fig. 5. pl. 07, fig.

12 Blackburn, 1942: 110. Stechaw, 1925:

260. Ralph, 1961b: 65, fiz. 9. Shepherd

& Watson, 1970; 140.

Recards: R, 24-33 m, an ascidians, bryozoa-

and Carpopeltis phyllaphera.

Material: Sparse infertile colonies. Stems to 1

om long.

Remarks: The stems are short, with closely set

hydrocladia and robust hydrothecae, features

characteristic. in this species, of an ocean en-

vironment.

Thecocarpus divaricatus (Busk) var. maccoyi

(Bale. 1884: 162, pl. 15. fig, 7 pl. 17, fig,

7), 1915: 312, pl. 1.

“Avlaophenia maccoyi Bale, 1882: 36, pl. 14,

fig. 2. Blackhiirn, 1942: 110,

Thececarpus divaricates CBusk). Shepherd &

Watson, 1970: 140,

Records: R, 23-45 m; §, 4-12 m, on Meta-

goniolithon charoides, Plocamium cartila-

gine, Acrocarpia paniculata and Zonaria

splralls.

Material; Luxuriant fertile colonies. Srenrs

short, ta 4 cm long, given off in groups from

a winding hydrorhiza, Proximal region of stem

without hydrocladia, lightly fascicled, some af

the supplementary tubes running up the main

stem for u short distance then branching. off.

Aydrocladia 4 mim long. Hydrathecue close-set

at 45° to hydroclacial axis, marginal teeth

deeply cut, the second anterior pair outwardly

bent, the unpaired anterior tooth — well

developed, the hatchet shape becoming mare

pronounced distally ylong the branch, Median

nemidothece vatlable in length, just over-

tapping margin in proximi region af hydro-

eladium, increasing to twice the height of

hydrathecs distally, standing well out fram: the

margin. the terminal aperture af the sume

time broadening out into 2 lobes. Corhulae

immature, with 4-11 pairs of gonohydroctladia;

immature gonophores in corbulae with more

than 10 Ieafiels. Cofour—variable, light to dark

brown.

Thecocarpos divarticatus {Busk) var, brigesi

Bale. 1926: 22. fix. 5.

Aglaophenia divaricatr (Busk).

162, pl. 05, fig. 8, pl, 17, fig. 7,

Balu. 1884:

E. WATSON

Aglaophenic ditaricata vay. acanthocarpa’ Bale,

1915 FIZ.

Records: R, 24-33; 8. 18 m, on fragments

of red alge and Canlerpe simpliciusente:

Stn. F, 65 m, on Syniplectoseyphus subdicho-

TOTTER,

Material> A few infertile stems in each colony.

Srenis to 1.5 em long, unbranched, mono-

siphonic, given olf singly from a winding

hydrorhiza, Hydrocladia flexuous. distant, cach

internode with 2 distinct seplu. Aydrothecar

with 4 pairs of marginal tecth. similar in shape

and size, the median anterior tooth net well

developed. Median nemutoiheca slightly lenger

than hydrotheca, following curve of the ab-

cauline wall, becoming erect just behind mar-

gin. terminal orifice round. in some cases

broadening tnto Iteral lobes; canting nemuato-

thecae larger than laterals, bent around stem,

orifice facing posteriorly, (nfaue—hrown.

Remarks: This is the first record of the vat.

hriggsi from §, Aust, (Other locality. Port

Jackson, N.S.W.).

Thecocarpus divaricatus (Busk} var. cystifera

Bale, 19157 314,

FIG. 72

Records R, 24-33 m, 8, 24 m, epillthle on

vertical rock faces,

Material: Abundant. infertile calonias. Colonies.

of 1-3 stems to 10 cm bigh, growing from a

small Common fibrous rootstock, Stenry thick.

woody. brittle, lightly fascicled, the poly-

siphonic tuhes running up the main stem and

branchng out alternately in one plane, giving

the colony a distinct "front and back” aspect

Proximal region of stem barc, showing sears

where brinches and hydrocladia have dropped

off. Aydrocladia to 13 mm long. Hvdrethecie

set al an angle of 45° to hvclrocladial axis; mar-

final teeth of similar size. evenly spaced. the

sinus between often wide wnd shallow. Median

neinatorheca following curve of the abcaulinc

wall. Lenminating just below margin, terminal

orifice round; cauline nematothccae large, ege-

shaped, Colonr—iight brown,

Remarks: Bale (1915) described; but did not

figure the variety eystifera. distinguishing it

from other varieties of T. divaricatus only on

the presence of the enlarged caine nemato-

thecae,

Remarks an the varieties af T. divaricatus:

Tt is of interest that the 3 varieties of this

species, recognized by Bale, ale recorded for

the first lime fram one Jocality, 7. muceovi

ELYDROIDS.

has previously been reported from various

localities along the Victorian coastline (Bale

1884) and from South Australia (Blackburn

1942. Shepherd & Watson 1970). T. cystifera

has been recorded only from) South Australia

(Bale 1915) and 7. hriggsi only from New

South Wales (Bale 1926). The only informa-

tion hitherto available on the macrostructures

of the hydrocaulus is given by Bale (1884)

who described the typical form as having

“numerous divergent branches and very dark

colour” and the var. meccoyi as a “dwarf

form”. (The larger “typical” form, ic. A,

divaricata Busk, a very common and distinctive

species of the south-eastern Australian coasi-

line, was not found al Pearson [., despite

careful search). The distinction between the

varieties has therefore Jargely rested on micro-

structures alone.

195

Although some intergradation in structure

does exist between the varieties, the material

from Pearson I. now enables a clear distinction

to be made in both micro- and maero-siruc-

lures, as Well as environmental preferences. T-

maccoyi and T, brigyysi, because of their simi-

larity in size and overlap ot substrate prefer-

ences, are difficult to dlistinguish in the field, but

they are easily separated on micro-structures:

T. cystifera although unmistakable im size and

growth habit, has hydrothecae almost identical

with those of I. briggst. T. maccoyi was the

only Variety fertile at the time of collection.

The gradation in micro- and macro-structures,

habit, and apparent difference in fertile season

of the varieties, suggests incipient speciation

within the 2. divaricamus group, Distinguishing

features between the varieties from Pearson I,

aré tabulated below.

T. maceeyi

medium, 4<¢m

lightly fascieled,

branched

twice length of hydra-

theca, orifice lobed

Stem length

Colony

Mesial nematotheca

Cauline nematotheca normal size, shape

Marginal teeth sharp, deep

Habit epiphytic

T. cystifera

large, 10cm

T. briggst

small, 1.5 cm

unfascicled, unbranched

to hydrothecal margin,

orifice round to lobed

Fascicled. braiched tn }

plane

to hydrothecal margin,

orifice round

normal size, shape, large, ovale

facing posteriorly

sharp, deep wide, shallow

epiphytic-epizoic epilithic

Lytnearpus mulderi (Bartlett, 1907),

FIG, 73

Aplaophenia muldert Bartlett, 1907; 66, Mulder

& Trebilcock, 1916: 73, pl, 10, fiz. 3-

Records: Among algae; no other data re-

corded.

Material: A fragment | em long, the distal end

of a fertile stem. The specimen conforms. to

vescriplions of Bartlett und Mulder & Trebil-

cock. Gonosome comprising 2 gonophores—t

male and 1 female, in an open corbula arising

from a primary hydrocladium. Primary hydro-

ciasdium with thecate proximal internode, fol-

towed by a swollen internode hearing 3. nema-

tocladia and gonophores. Nematocladia 0.75—

(.84 mm long (but may be broken) each bear-

ing a single row of nematothecae. Ganothecae

round, laterally compressed; female, 135 mm

in diam., slightly larger than male, packed with

mature ova, blaslostyle almost filling ganothecal

cavity: male gonophore surrounded by a blasta-

styit o£ the samé shape, but of smaller size

than the female.

Remarks; This is the first record of a species

referahle 10 the genus Lytecarpuy from

southern Australian waters. As earlier descrip-

tions wete derived from fragmentary infertile

material, it was assumed, in the absence of the

gonosome, to belong to the closely related

genus Apglaophenia, common in southern Aus-

tralia, This is the vhird record of this rare but

distinctive species, and the first record for S,

Aust, (Other locality—Bream Creek, Vic.).

Halicornopsis elegans (Lamarck, 1816). Bale,

tda: 56; 1915: 303. Briges, 1914:

309, Blackburn, 1942; 107. Shepherd &

Watson, 1970; 140,

Plamiularia elegans Lamarck, 1816; 129,

Halicornopsis aviculuris Bale, 1882: 26, pl. 13,

fig. 3; 1X84: 185, pl. 10, figs. 1. 2. pl 19, fig.

32.

Records: R, 33 m, epilithie, and on bryozoa

and red algae.

Material: One small infertile colony. Stems Lo

3.cm long. branched,

Remarks: Vhe colonics were comparatively

small and the individuyl stems short for the

species,

JEANETTE E. WATSON

196

O.5mm

wus 'o

wusz:-O

wuUgrd

wu Q-2

HYDROIDS (97

Halicornaria longirostr® (Kirchenpauer, 1872).

Bale, 1884: [8]. pl. 13, fig. 7, pl. 16, fig.

3, pl. 19, fig. 30. Shepherd & Watson,

1970; 140.

Apgloophenia flongirastris Kirchenpauer,

28, pl. 1, fig. 19, pl. 5, Ng. 20,

Records: KR, 18-33 m, cpilithic on rock walls,

oo Herainunia memus, red algae, and bryo-

zoa,

Material: Abundant infertile colonies, Stems to

7 om long. with 1-2 proximal branches. Colour

—pale straw colour

Remarks! The colonies fall into 2 groups—

those with long stems, and those with short

stems, The larger colonies, comprising clusters

mt longer stems (up to 7 cm) were either epi-

lithic or epizoic, whereas the shorter stems Cup

tu 3 cm) growmg singly, were epiphytic on

algac. There is no difference in micro-structures

between these two ecologically distinc, stem

types.

Halicornaria prolifera Bale, 1882: 34, pl. 14,

fiz. 5; 1884: 183, pl). 14, fig. 1, pl. 16, fig,

10, Ritchie, 1911; 858, pl, 85. figs, 2, 3.

Records: R, 30 m, epilithic.

Marerials One infertile unbranched colony.

Stem & cm high, Aydrocledia 0.7 mm long.

given off at un acute angle to the stem. Anterior

and posterior cauline nemutothecae with 3,

somerimes 4 orifices, median hydrocladial

nematotheca extending just below thecal mar-

gin. Marginal teeth shallowly scalloped, the

middle pair slightly everted.

Remarks: The specimen agrees in most respects

with Bale’s description of H. prelifera, except

that the median nematothecue ae a little

shorter than those described by Bale, and all

the cauline nematothecae have 3 orifices. The

hydrothecal margin is circular in anterior view,

similar to Ritchic’s (1911) specimens. This is

the first record ol H. prolifera from S. Aust,

(Other localities—N-S,W. and Vic.)

Halicornaria auren 1sp-

1&72:

material, remainder of holotype colony—R,

33 m, epilithic on rock walls; paratypes,

Gi089, microslide, G2108, preserved

material, remainder of colony—R, 33 m,

epilithic; G2090, microslide, G2109, pre-

served material, remainder of colony—R,

27-30 m, epilithic on rock walls; SAM

microslide.

Dexeription from holotype: Colony 6 em high,

growing from a smail fibrous rootstock, Sent

monosiphonic, lower stem 1 min in diam,, athe-

cute. divided inte internodes, nodes transverse,

proximal intemodes wath circular pits where

cauline nemuiethecue huve dropped off. First

branch 2 cm abuve base, all branching there-

after dichotomous, at an angle of about 40°,

the branches becoming somewhat convergent

distally, then rebranching, Branching repeated

6-7 Times, always in the une plane. Branch

internodes short, 0.60-0.69 mm, divided hy

indistinct transverse nodes, diam, at node,

0.66-0.84 mm. AHydraciadi2 to 5 mm long,

alternate, 2 on an internode, given olf after

first branching of main stem, standing out

stiffly at an acute angle from the branch, giving

the colony a decidedly “front and back” aspect.

Hydrocladial internudes 0.28-0.31 mm long,

nodes almost perpendicular to the axis, indis-

tinct, no internodal septa, Hydrothecae squat,

set. at an angle of 50° to hydrocladium, 0.23—

0.26 mm deep, filling internode; adcauline wall

straight, fixed part 0.12-0.14 mm long, free

part 0.03-0.05 mm long; abcauline wall 0,t7—

0.19 mm long, divided in the middle by a long

intrathecal ridge projecting slightly forward

more than half way across thecal cavity; base

of bydrotheca flat, with a small knot of den-

ticles on the adcauline side marking the hydro-

pore, Margin (.17-),29 mm in diarm., with 8

teeth—3. pairs of prominent blunily pointed

teeth, the middle pair the longest, outwardly

hent, the anterior pair erect. the posterior pair

slightly everted: 1 low postenor tooth, often

chsolete. and 1 small anterior tooth below the

median nematotheca. Median nematothecue

almost twice the height of the hydrotheca,

0.28-0.40 mm jong, 0.05-0.07 mm wide at

FIGS. 74-76

Type Moterial and Records; Holotype, NMV

G2088, microslide; G2107. preserved

Figs,

#8-71. Plumularia australiensis usp. Fig. 6%.—Part of stem. Fig, 69.—Part of hydrocladium, en-

larged. Fig. 70.—Male gonotbeca, (Figs. 68-70 from holotype), Fig, 71—Female eonp-

theca, from paratype.

Fig. 72

to shaw cauline nematothecae.

Fig 73.

Figs. 74-76

Thecoéarpus divaricatus var, cystifere. Bale. Part. of branch with hydrocladia removed

Lytocarpus mulderi (Bartlett), Open corbula with male and female gonophores.

. Halicorseria aurea op. From holetype, Fig, 74.—Part of stem wilh hydrocladia on one

cide removed ta show cauline nematothecae, Fle, 75. —Hydrothecae. anterior view, Fig,

76,.—Hydrothecsa¢, Jatersl view-

198 JEANETTE EB, WATSON

hase, tapering distally and inclined forward,

lerminal apeyture small, circular, lateral aper-

ture distinct, Lateral neiatothecae small, 0,1 1—

O13 mm long, saccate, not reaching thecal

margin, | small terminal aperture on aw short

outwardly turned neck, and 1 lateral aperture

facing inward towards the hydrotheca. Gono-

theca absent. Colaur—amber,

Remarks: The matginal thecal teeth exhibit the

variations in Jength and shape characteristic of

Halicorrnaria. The teeth are normally long, the

middle tooth being the longest of the 3 on each

side. The median nematothecue are all of

newly equal size, and show little tendency

towards increase in length in the distal region

of the hydrocladium.

A. aurea resembles 2 other southern Austra-

lian species of Hallcornaria—H. superba Bale,

and #f.. baileyi Bale. Tt differs from the former

in minor micro-structures, the marginal thecal

teeth of H. superba beng sharper and narrower

than those of I, aurea, the median nematu-

theca of H. superba is larger, and the lateral

nematothecae have 1 Jateral and 2 terminal

uperiures. In A. aurea the Ioterals have only

2 apertures, i facing inward and the other out-

ward; as they are very small they are sometimes

difficult to distinguish, In mucroe-structures,

however, H, aurea is easily distinguished from

Hi. superba, whose stems are long, gracefully

pluiyosc, and yellow-green in colour. In size,

growth hubit, and colour. the colonies af H.

area are indistinguishable from AH. baileyi,

‘they are however, quite different in micro.

structures,

ff, aurea is an abundant species on tock

faces exposed to surge.

Acknowledgments

Jam grateful to the Royal Society of South

Australia and the Department of Fisheries und

Fiuuna Conservation of South Australia for the

Opportunity to participate in the Pearson Island

Expeuition; to the Director and Dr. B. J. Smith

of the National Museum of Victoria, Mel-

boume. Jor use of facilities and equipment; to

Dr. H. B.S. Womersley, Botany Department.

University of Adelaide, for identificaGon and

information on algne, and helpful.advice; to the

Australian Museum for the loan of material,

and to Mr. S.A. Shepherd for criticisin of the

manuseript. Thanks are due to Normalair Gar-

fet, Melbourne, for the loan of a compressor.

L especially acknowledge the unfailing help and

enthusiasm of my diving companions, Scoresby

A, Shepherd, and John O, Ottoway. Expenses

of this study were partly met by a gruna fram

the Science & Industry Endowment Fund,

CSIRO,

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PEARSON ISLAND EXPEDITION 19697-10. OPISTHOBRANCHS

BY ROBERT BURNS*

Summary

BURN, R. (1973). -Pearson Island Expedition 1969.-10. Opisthobranchs. Trans. R. Soc. S.

Aust. 97(3), 201-205, 31 August, 1973.

Three species of opisthobranch molluscs from Pearson I., Notarchus indicus (Schweigger),

Aporodoris merria Burn n.sp. and Goniodoris meracula Burn, and one species from nearby

Flinders I., Sagaminopteron ornatum Tokioka & Baba, are new records for South Australia.

Additional distributional data are given for G. meracula and S. ornatum.

PEARSON ISLAND EXPEDITION 1969+—10. OPISTHOBRANCHS

by Rogert Burn*

Summary

Burn, R. (1973).—Pearson Island Expedition 1969.—10. Opisthobranchs. Trans. R- Soc. 8.

Aust. 97(3), 201-205, 31 August, 1973.

Three species of opisthobranch molluscs from Pearson I., Notarchus indicus (Schweigger),

Aperodoris merria Burn usp, and Goniodoris meracula Burn, and one species from nearby

Flinders I, Sagaminopteroa ornatum Tokioka & Baba, are new records for South Aus-

tralia. Additional distributional data are given for G. meracula and S. ornatrm.

Introduction

The opisthobranch molluscan fauna of South

Australia is relatively poorly known, especially

with regard to the naked or “nudibranch”

species Of the western coastline of the State..

Thus it is not unexpected that any collection

from this atea should contain new species and

new records,

Three species described in this paper were

collected during the 1969 Pearson Island Ex-

pedition, organized by the Royal Society of

South Australia and the South Australian De-

partment of Fisheries and Fauna Conservation.

The Pearson Islands are the small southern

part of the Investigator Group at the eastern

end of the Great Australian Bight. The largest

island, Pearson I, is about 162 hectares in

extent, but the others are much smaller; they

lic 64 km southwest of Elliston.

The fourth species im this paper was

collected during a stop-over by the Expedition

at Flinders T., a large island that forms the

northern part of the Investigator Group.

The specimens have been deposited in the

National Museum of Victoria, Melbourne

(NMV).

Order CEPHALASPIDEA

Superfamily PHILINACEA

Family GASTROPTERIDAE

Sagaminopteron ornatum Tokoika & Baba,

1964: 218. Bennett, 1966: pls. 1, 120b.

Baba, 1970: 47.

FIGS. 1-2

Material: Flinders I, Jan, 1969; 2 spect-

mens from 10 m on C'ystophora on vertical

rock face in fair surge (NMV. F27399).

The living animals were reported as “hright

blue under water, parapodia edged with bright

yellow”. They are now colourless and 12 and

9 mm long, 6 and 5 mm broad. When alive,

the larger animal was almost 25 mm long.

The one major difference between the

Japanese type specimens and Australian

material (Fig. 1) is the presence of a relatively

large strong shell in the mantle cavity beneath

the posterior caudal lobe of the body. The

shell of the larger Flinders J, specimen (Fig. 2)

is 2 mm Jong by 1.4 mm wide, and is white

with a yellowish transparent protoconch, the

interior of which is open. The shell of a Lord

Howe I, specimen is 2.4 x 1.7 mm, one from

Cockburn Sound, Western Australia, is 2.1 x

1.6 mm, and another from Heron I.. Queens-

Jand, is almost 4 mm long,

Tt must be assumed that the shells of the

Japanese types dissolved during fixation and

preservation.

Though hitherto unrecorded, Sagaminap-

teron ornatum 3s ia fairly common species in

eastern and southern Australia. Specimens

examined by the writer are:

1. Lord Howe 1L—Middle Beach, Jan. 1959,

R. R. Rlackwood, 1 specimen (NMY,

F20717).

2. Queensland.—Heron 1., Capricorn Group,

Aug. 1965, I. Bennett, | specimen. Humpty

* Honorary Associate, National Museum of Victoria, Melbourne, Vic. 3006.

+ Other accounts of the geomorphology and biology of the Pearson Islands are given in

Volume 95, Part 3 (1971) of the Transactions, as wel] as in the present Part,

22 R. BURN

L, Keppel Group, Supt, 1969, N, Coleman, These specimens were collected from be-

1 specimen. tween the intertidal zone and 20 m depth,

3. New South Wales —Angourie, Aug. 1966, from heneath boulders, from brown algae,

A, A. Cameron, 1 specimen. Minnie or from grey branching sponges. They have

Waters, Jan, 1963, G. Biddle, 1 specimen. often been observed, in rock pools and deeper

Bawley Point, near Ulladulla, Dec. 1963, water, to swim with a rapid synchronous un-

f. Bennett, 3 specimens. dulution of the parapodia.

4, Victoria—Bear Gully, Waratah Bay, April

1970, f. Marrow, 6 specimens. Order ANASPIDEA

5, South Australia—Port Noarlunga, Feb, Family APLYSHDAK

1966, R, Balfour, 1 specimen (SAM, Notarchus indicus Schweigger, 1820. Bergh,

14888). Anxious Bay, Dec. 1968, T- 1902: 349. Engel, 1936; 113. Eales,

Castle, 1 specimen. 1944: 12.

6, Western Australia—West of Carnac |,, FIGS. 3-6

Cockburn Sound, Feb. 1971, B. R. Wilsan Material; Pearson [., Jan. 1969, 1 specimen

& N. Coleman, 4 specimens (WAM, 474- from algae on horizontal faces at 26 m

71). (NMV, F27401).

Figs, 1-2. Sagaminopteron ornatum. Fig. 1— Dorsal view of a 20 mm long specimen from Port

Noarlunga, S. Aust., from a sketch by Dr Helene M, Laws, Curator of Marine Inverte-

brates, South Australian Museum. Fig, 2—Shell from larger Flinders I. specimen, dimen-

sions 2 x 1.4 mm.

Figs. 3-6. Notarchus indicus. Fig. 3.—Diagram of mantle cayity and aperture (a—anus, b—dgill,

c—pigment gland, d—mantle apertute, e—opaline gland), Fig. 4—Radular teeth, Fig. 5,—

Jaw element. Fig. 6—Male copulatory organ (p—penis, r—retractar muscles, s—sheath,

t—seminal groove).

OPISTHOBRANCHS

The colourless preserved specimen is 5 mm

jong, 3,5 mm wide and 3 mm high, Fhe head

and neck are invaginated into the smooth vis-

ceral hump. The 1 mm long mantle aperture

(Fig, 30), of che usual external shape, is placed

well forward, The large mantle cavity, not yet

pervious with the dorsal mantle aperture, con-

tains a small lobulated gill (Fig. 3b), a Jong

loop of the intestine terminating well behind

the gill stem at the anus (Fig. 3a), a long

curved granular pigment gland (Fig. 3c}, and

a small white opaline gland (Fig. 3e). No

genital groove is apparent, Short stumpy

thinophores with deep lateral grooves project

fram the head, and a small rounded knob-like

oral tentacle occurs ether side of the mouth.

The jaw elements (Fig. 3) are narrowest

just below the serrulate distal end. The hyaline

radula (Fig. 4) is almost 2 mm long with 21

rows of 20.1.20 teeth. The rhachidian tooth is

slender with sharply pointed cusp and a short

denticle each side. The lobulate first lateral

tooth has onc inner and two outer denticles,

and the next six teeth have op to lwo inner

and four outer denticles, The succeeding teeth

have longer cusps with up to five inner and

nine outer denticles at the third or fourth tooth

from the margin, The murginal tooth has one

innee denticle well back from the tip and

about four incipient outer denlicles,

The minitile male copulatory organ (Fig.

6) agrees exactly with the figure for Mauritius

specimens given by Engel (1936, p. [16, fig.

4) with the exception that the grooved smooth

penis hys not as many spiral turns.

Discusion: The descriptions by Bergh (1902)

and Engel (1936) of specimens From Mauri-

tius, plus that of a specimen from Zanzibar

(Eales 1944), satisfactorily diagnose Nofar-

chax indicus, The spiral unarmed penis justi-

fies the identification of thts very small Pear-

son T. specimen. The smal) number of lateral

teeth ¢20), the marginals of which are not

slender and smooth, does not agree with the

above three descriptions where the lateral teeth

number 43-45, 33 and 32 respectively and the

marginals are long: slender and smooth. How-

ever, the Pearson I. specimen is probably a

juvenile in which the radula has not attained

the full complement of teeth nor the penis the

full number of turns,

Notarchus indicus has a wide Indo-west

Pacific tropical and subtropical distribution,

and hag been recorded from Sydney Harbour,

New South Wales (Engel 1936, p. 119}. It as

w new record for South Australia,

205

Order DORIDACEA

Tribe CRYPTOBRANCHIA

Family DORIDIDAE

Aporodorls merria n.sp.

FIGS. 7-11

Material: Pearson J., Jan. 1969, | specimen

(holotype) from red algae at 52 m (NMV,

F27402).

The alcohol preserved specimen (Fig. 7) is

dull orange-fawn in colour. It measures & mm

long, 5 mm broad and 3.5 mm high. The

notum is covered with various sized tubercles

(Fig, 86), the largest. of Which are somewhiut

flay clavate and up te 0.6 mm in diam, All

tubercles have projecting angles both laterally

and dorsally. Bundles of spicules strengthen

each angle. The rhinophorsl cavities are pro-

tected by four tubercles; a large one ot each

side, a sniall one in front and a small one be-

hind each cavity (Fig. 8a). The branchial

cavity has nine or ten lappet-like tubercles of

various sizes along the margin (Fig, 8¢); these

tubercles are Up Lo 1 mm tong and 0.8 mm

wide and have small projecting angles or

Points on the onter or dorsal face only.

The thick fleshy hyponotum is narrower than

the foot (Pig. 9), from which it is separated

laterally by little more than the foot margin.

The genital aperture opens in the middle width

of the hyponotum. The lamellate Thinophores

are completely withdrawn. There are five mul-

tipinnate gills. The head (Fig, 10) lies within

a deep concavity of the anterior hyponoeuim,

with a grooved ridge-like oral tentacle at each

side of the mouth. The broad font is anteriorly

truncate with the upper lamina leading into

the head cavity where it. is notched, The tail is

thin and broadly rounded.

The thick labial cuticle ts smooth. The

radula is 1.7 mm long and 1.4 mm wide. It

has 40 rows of 41 teeth per half row, All teeth

are hook-shaped und bear a single outer

denticle beside the cusp, except for the two

marginals which have If or more comb-like

denticles (Pig. 11).

The brittle genital organs could not be

examined satisfactorily, The whitish sompulla

is long and winding. The yellow vas deferens

is short and twisting; and terminates in an un-

armed penial sheath without penial papilla.

Discussion: The angular, flattened, clavate

tubercles of the notam and the single promin-

ent outer denticle of the lateral radular teeth

separate A. nrerria from other species of

Aporodoriy Ihering, (886, The unarmed penis

of the new species is similar to that of THor-

204

disa Bergh. 1877, but in that genus the Jateral

teeth are smooth. The radula is also similar to

that of Taringa Marcus, 1955, but the un-

armed penis of A, #erria contrasts with the

cuticularized penial papilla and spines of the

former genus.

The concavity of the head and the large

lappet-like tubercles of the branchial margin

ure further distinguishing characters, The rela-

tively flat underside of the specimen, with the

head parts recessed, suggests that A. mierria

has unusual feeding preferences.

The specific name is derived from “merri”,

an Australian Aboriginal word meaning stones,

in allusion to the notal tubercles.

Figs.

R. BURN

Tribe PHANEROBRANCHIA

Superfamily SUCTORIA

Family GONIODORIDIDAE

Goniodoris meracula Burn, 1958: 27; 1966:

227,

FIGS, 12-13

Material: Off Dorothee, Jan. 1969, 1 speci-

men [rom algae at 65 m (NMV, F27400).

The colourless preserved specimen measures

7.5 mam long and 3,5 mm broad. Living speci-

mens (Fig. 12) are usually yellowish with

darker brown mottling. Important characters

for the identification of this species are the

smooth body, the high notal flange open be-

lateral =

7-11. Aporodoris merria. Fig, 7—Dorsal view of preserved holotype. Fig. §—Notal tubercles

from rhinophoral cavity (a), middle of the notum (b), and branchial margin (c). Fig.

9.—Anferior hyponotum. Fig, 10.—Detail of head with anterior foot folded down, Fig,

11.—Radular teeth,

Figs. 12-13. Gonivdoriy meracuta. Fig. 12.—Dorsal view of an $ inm long specimen from Point Dan-

ger, Torquay, Vic. Fig. 13—Half row of radular teeth from Sydney Harbour specimen,

OPISTHOBRANCHS

hind the gills, the short caudal crest, and the

seven gills.

The species has been very rarely collected.

The holotype was found eating into a yellow-

ish compound ascidian beneath a. stone at Point

Danger, Torquay, Victoria (Burn 1958), and a

second specimen was recorded from Portsea

Pier, Port Phillip Bay (Burn 1966). A third

specimen was taken by the writer at Point

Danger, Torquay, Dec, 1963, where it was

crawling on brown algae.

Three specimens (Australian Museum,

C312), dredged in Sydney Harbour, New

South Wales, on |! June 1892, are a new

record for that State and the only other speci-

mens known to date. Each measures 10.5 mm

205

long by 5.5 mm wide. The radula (Fig. 13)

of one specimen has the formula 26 x

1,1,0.1.1; the lateral tooth is strongly hooked

with smooth cusp, while the marginal tooth

has much the same shape and is about half.

the size of the lateral tooth.

Goniodoris meracula is a new record for

South Australia.

Acknowledgements

The writer is indebted to Mrs Jeanette E.

Watson, Honorary Associate, National

Museum of Victoria, Melbourne, for the col-

lection of, and the ficld notes on, the Pearson

I. opisthobranchs. This research has been aided

by a grant from the Science and Industry En-

dowment Fund, C.S.I.R.O., Canberra.

References

Baba, K. (1970) —List of the Gastropteridae and

Runcinidae of Japan. Collecting and Breed-

ing, 32(2), 46-48 (in Japanese).

Bennetr, EL (1966).—"“The Fringe of the Sea.”

(Rigby: Adelaide, )

BercH, R. (1902).—Malacologische Unter-

suchungen. Jn C. Semper (Ed.), “Reisen im

Archipel der Philippinen", Vol. 7, pp. 313-

382, plates 25-29.

Burn, R. (1958).—Forther Victorian Opistho-

branchia. J. Malac, Soc, Aust. 1(2), 20-36.

Burn, R. (1966).—Port Phillip Survey 1957-

1963: Ophbisthobranchia. Mem. natn. Mus.

Vict. 27, 265-288.

Eaues, N. B. (1944).—Aplysiids from the Indian

Ocean, etc. Proc, Malac. Soc. Lond, 26, 1=

ENGEL, H. (1936).—Some additions to our know-

ledge of the genus Notarchus, Proc. Malac.

Sac. Lond, 22, 113-119.

Toxioxa, T., & Basa, K. (1964).—Four new

species and a new genus of the family Gas-

tropteridae from Japan. Publs Sete Mar,

Biol. Lab. 12(3), 201-229, pls. 10-13.

PEARSON ISLAND EXPEDITION 19697-11. CRUSTACEA: ISOPODA

BY W. F. SEED*

Summary

SEED, W. F., (1973) .-Pearson Island Expedition 1969.-11. Crustacea: Isopoda. Trans. R.

Soc. S. Aust. 97(3), 207-212, 31 August, 1973.

Eleven species of isopods, all sphaeromatids, are represented in a small collection from Pearson I.

Of these species, two are too immature for specific identification, but belong to the genera

Exosphaeroma and Cymodopsis. One new species, Cilicaeopsis floccosa, is described and figured.

The previously-known species are: Cymodoce gaimardii, C. pubescens, C. unguiculata, Cilicaea

latreillei, Cerceis acuticaudata, Haswellia anomala and H. cilicioides.

PEARSON ISLAND EXPEDITION 1969;—11. CRUSTACEA; ISOPODA

by W. F, SEED*

Summary

Seep, W. F., (1973}.—Pearson Island Expedition 1969.—11. Crustacea: Isopoda. Trans. R.

Soe. §. Aust, 97(3), 207-212, 31 Angust, 1973.

Eleven species of isopods, all sphaeromatids, are represented in a small calection from

Pearson I. Of these species, two are too immature for specific identification, but helong to the

genera Exosphacroma and Cymeodopsis. One new species, Cilicaecpsis floccosa, is described

and figured. The previously-known species are: Cymodace gaimardii, C. pubescens, C. ungui-

culata, Cilicaea latretilei, Cerceix aculicaudata, Huswellia anomala and H, cilicioides.

Introduction

This paper discusses the isopod crustaceans

collected during the Pearson I. expedition of

6-13 January, 1969, sponsored jointly by the

Royal Society of South Australia and the De-

partment of Fisherics and Fauna Conservation

of Soutb Australia. For discussion of collecting

siles see Shepherd & Womersley (1971) and

Watson (1973); R and § indicate rough-water

and sheltered localities.

All specimens Were recovered during the

sorting of algal collections made by divers

(8. A. Shepherd, J. EK. Watson and J. Otta-

way), This may account for the immaturity of

much of the material, smce larger, and pre-

sumably more vigorous, animals are often ob-

served to escape the net during collection

(S. A, Shepherd, pers, comm.). Nine species

(including one new species) are identified, and

two Species are diagnosed to genus only,

The keys of Hale (1929), Hansen (1905)

and Hurley (1961) were used to identify the

genera; most of the speciés were determined

fram Hale’s (1929) keys and species descrip-

tions. Syhonymies ute not necessarily com-

plete. | have followed Menzies (1962; see also

Menzies & Frankenberg 1966) in giving only a

bricf diagnosis of the new species, supported

by accurately drawn figures.

Use of the name Sphaeromatidae (rather

than the more commonly-used Sphueromidae)

follows Schultz (1969) and Naylor (1972),

and anticipates a forthcoming paper by Hurley

& Jansen (pers. comm.) in which the usage ts

discussed,

Specimens are deposited in the isopod cal-

lection of the National Museum of Victoria,

Melbourne (NMV), but only the new species

has been registered.

Tribe FLABELLIFERA

Family SPHAEROMATIDAE

Group HEMIBRANCHIATAL

Genus EXOSPHAEROMA Stebbing, 1900

Exosphaeroma sp-

Locality: Pearson I. (Station F at 65 m),

Material: One immature male, damaged

(about 5 mm long). Penes are developing

but appendix masculina is not yet distinct.

Remarks: More than thirty species have been

placed in this genus, and the specimen differs

from all of them in at least one point: the

uropodal exopod is W-shaped at the distal end,

Description of this species must await more

suitable material.

Genus CYMODOCE Leach, 1813-14

Cymodoce gaimardii (Milne Edwards). Han-

sen, 1905: 121, Baker, 1926: 256, pl,

42, fig. 2. Hale, 1929: 286, fig, 284.

Nierstrasz, 1931: 200. Naylor, 1966: 186.

fig. 2.

Sphaeroma gaimardii

1840; 209,

Milne Edwards,

“Department of Applied Biology. Royal Melbourne Institute of Technology, 124 fa Trobe

St.. Melbourne, Vic. 3000.

* Other accounts of the geomorphology ard biology of the Pearson Islands are given in

Volume 95, Part 3 (1971) of the Transactions, as well as lhe present Part.

208

FIGS, 1-4

Localities: Australia (Milne Edwards 1840);

Vic.: Port Phillip Bay (Baker 1926, Nay-

lor 1966); Tas,: (Baker 1926); S. Aust:

Encounter Bay, Gulf St. Vincent (Baker

1926), New record: Peurson |. (Station F at

65 m).

Material; One female (11 mm long), im-

mature, With no oostegites or eggs, and the

mouthparts unmodified.

Remarks: The specimen agrees with the des-

criptions and figures of Baker (1926) and

Naylor (1964), allowing for is being a

juvenile. Comparison with these figures and

with specimens collected from Western Port

Bay reveals variation within the species in the

sharpness of truncation of the uropodal endo-

pods, in the shape of the joint between telsonic

and pleonic tagmata, and in the shape and

degree of exposure of the anterior suture on

the pleon (Figs. 1-4).

Cymoaduce pubescens (Milne Edwards). Han-

sen, 1905; 122. Stebbing, 1910: 104,

Nierstrasz, 1931: 198. Naylor, 1966:

188, fig. 3.

Sphaeroma pubescens Milne Edwards.

1840; 209,

Paracilicuew (2) pibescens (Milne Ed-

wards), Baker, 1926: 262, pl. 43, figs.

8-11; pl. 48, fig. 1. Hale, 1929: 290_

Locatlties: Austrilia (Milne Edwards 1840);

WN,S.W.: Port Jackson, Port Stephens (Has-

well 1882); Vie.; Port Phillip Bay (Nuylor

1966), Zanzibar: Wasin (Stebbing 1910),

Indonesia: Sailus Besar, Paternoster 1.

(Nierstrasz 1931), New record: Pearson 1,

(Stution F at 65 m),

Material; One mule (8 mm jong) and one

female 7.5 mim long), both immature: the

W. F. SEED

appendix musculina of the male is not lree,

the female has no oostegites Or eggs, and its

mouthparts are unmodified.

Remarks; Specimens agree with published des-

criplions of this species. It should be noted

that, although Hale (1929) has followed Baker

in referring this species to Purarilicaea im the

text, his key agrecs with those of Hansen

(1905) and Hurley (1961), the species key-

ing out to Cymedece in all three.

Cymodoce unguiculata Barnard, 1914: 394, pl.

34B. Baker, 1926; 259. Hale, 1929: 285.

Localities: South Africa (Barnard 1914),

S, Aust.; Beachport (Baker 1926), New

record: Pearson I, (Station F at 65 m).

Material; Two feniles (6 and 9 mm long),

both immature, without eggs or modification

of the mouthparts, but with four pairs of

oostegite buds in the larger specimen,

Remarks: The specimens Jack the marginal

fringe of setae referred to by both Hale and

Barnard; the bosses on the telson are much

less prominent than Barhard's figures indicute

(by inference from his description, and

directly from Hale's. they are the same size in

adults of both sexes); and the hooked uro-

podal exopad differs slightly in both specimens

from Barnard’s figures, The uropodal endo-

pod, however, is. slightly excavate distally, as

shown in Barnard’s figure of the female, and

in other Tespects the specimens agrée well with

desenptions of C. unguiculaia.

Genus CILICAEA Leach, 1818

Cilicaca curtispina Haswell, 1881b: 185, pl. 3,

fiz. 4. Stebbing, 1905: 36, Baker, 1908;

142, pl. 4, figs. 12-17, pl. 5, figs. 1-%;

1938: pl. 6, figs, 8-9. Hale. 1929; 280,

Figs. 1-4.

Cymodoce yaimardii, posterior region, Fig. 1.—Female (11 tm long) from Pearson T. Fig.

2 -Female (13.5 mm long) from Port Phillin (after Naylor), Fig. 3—Male (24 mm Jong)

from Western Porl. Fig. 4.—After Baker: "Prohably » young male"; locality and scale rot

Indleated,

CRUSTACEA; ISOPODA

fiz, 280. Nierstrasz, 1931, 205. Naylor,

1966; 189,

Naesa antennatliy

nomen nudum,

Cilicaea anrennaliy While Miers, 1884+

310,

Cilfcoaea = avitennalis = Miers,

1905: 335. Niersteasz, 1931: 205.

Localities; W. Aust.: Swan River (White

1847, Miers 1884) Vic.: Port Phillip

{Haswell 1881b. 1882; Naylor 1966); “very

common in shallow water around [southern

Australian] coasts" (Hale 1929). New

record, Pearson 1. (R at 25 m).

Material; Qne adult male (14 mm long).

Remarks: The specimen agrees with Baker's

(1908) and Hale’s (1929) descriptions, except

that the uropodal cxopods are ruunded

apically, rather than slightly bifid. No deserip-

tion tefers to the pads of short setue lining the

incurved inner surfuce of the distal part of

these cxopods and of the median projection.

This feature, together with the shape und

atrangement of these three projections, seems

to imply some definite function, such as clasp-

ing the female during mating, or clasping the

anterior region When the aninsal is rolled.

White, i847: 105;

Stebdbing,

Cilicaes Jatreillei Leach, 1818: 342. Miers,

1884: 308. Stebbing, 1905: 36, pl, 8,

Hiatle, 1929; 282, fiz. 282, Nierstrasz,

1931: 204. figs. 92-96, Naylor, 1966;

L90, fig. 3.

Neaesea latreiilei Milne Edwards, 1840:

218.

Cilicvea crassicandeta Haswell,

475, pl. 17. fig. 3-

Localities: There are numerous records from

South Africa, Ceylon, East Indios, Australia

and New Zealand [see Nierstrusz 193),

Naylor 1966). New recerd:; Pearson I. (R

at 20-25 m),

Material; Qne specimen, apparently female

and very young {6 mm),

Remarks: The females of Cymodoce pubescens

and Cilicaea latreitle’, both of which have bifid

twopodal exopods and are otherwise very simi-

lan. have caused much taxonomic confusion,

The Peurson I. specimen Jacks the characteria-

lic scale-sctae of Cymnoedoce pubescens, being

fairly liberally covered with stiff, erect setae:

it agrees well with Naylor's (1966) figure of

a female of Cilicaea latrejllei, although it has

not the well-defined anterior buss of the Port

Phillip (and Western Port) specimens, and the

posterior tip ef the uropodal exopod is forked’.

1881a;

abs)

These could well be juvenile features: com-

purison with a series of specimens from Wes-

tern Port leaves little doubt that it is a yery

young female of Cilicaea Jarreillei.

Jt must be noted thal the male figured by

Niesstrasz, despite his statement that “Die Tiere

(Figs, 92-96) stimmen put mit den Beschrei-

bungen von Miers [1884], Stebbing [1905], und

Barnard [1914] tiberein”, clearly belongs to

another species, and what he has labelled as

the female of C. latrei/le? is not a female of

that species, although it could he a Votng

male, Reliable figures will be found in the

papers by Barnard, Naylor and Stebbing; they

agree with all Victorian specimens available.

Genus CILICAEOPSIS Hansen, 1905

Hansen established this genus by designating

Cilleaca granulata Whitelegge (1902) as the

type, and his key to genera shows the diagnos-

tic characters to be; “Abdominal notch semi-

circular, without any vestige of mesial lobe.

ndp, of urp. rudimentary in the tale", This

seems to have been broudly interpreted as to

both the semicircular nature of the abdom-

inal notch and the rudimentary nature of the

endopod. Some of the species included in this

YeNUsS appear to necessitate a new generic diag-

nosis, but it will be best if modification of the

agnosis is left until this and the several

closely-related genera are reviewed.

Taking a broad view of the meaning of

semicircular, as Baker (1926) has done, the

new species described below conforms with

Hansen's diagnosis,

Cilicaeopsis flaccesa n,sp.

Locality: Pearson 1. (R at 25 ma: “From

algae on horizontal face”).

Material: One specimen, the holotype male

(median Jength 12,5 mm, total Jength 16

mm, width 6.1 min), wpparently adult, § A,

Shepherd, 10.i,1989 (NMY, J-249).

FIGS. 5-11

Diagnosis: Citicgeaopsis: with slender, curved

tropodal exopods beuring a Furry tuft of setae

on the median aspect of the distal end. Simi-

lur selae cover the dorsal surface of the endo-

pods and of the pleotelson below and behind

the two Jarge tuberculate bosses; surface else-

where glubrous. Appendix musculina Jong,

with a curved narrow tip extending well

beyond the setae of the second pleopod; inner

edge of the endopod grooved behind ta accom-

miodate the upper part of the appendix. Penes

long, tapering to a point. taterally compressed

and kinked backward near the end, Abdominal

W. F. SEED

Imm

FIGS, 5,6,7

5mm

FIGS. B. 9.

10, 11

Figs. 5-11. Cilicaeapsis floccosa. All figures from the holotype male. Fig. 5—Left maxillipede, Fig. 6.

—Left penis, from the right side, Fig. 7—Left second pleopod and appendix masculina.

Fig. 8.—Head, ventral view. Fig. 9. Whole animal, dorsal view. Fig. 10.—Posterior region,

from ihe left side. Fig. 11.—Pleotelson and uropods, ventral vicw.

CRUSTACEA: ISOPODA

notch wide and shallow, not visible from

above. Epistome pointed, much shorter than

broad.

Genus CYMODOPSIS Baker, 1926

Cymodopsis sp.

Lacalitys Pearson T, (R at 25 m, from algae

on horizontal face).

Material; One immature male (8 mm Jong),

with very rudimentary penes and appendix

masculina not yet appyrent-

Remarks: The specimen superficially resembles

Baker's (1926) figure of Cymodopsis crassa

in general form and in having two large coni-

¢al projections on the pleotelson. In lateral

yiew these are seen to be slightly undercut

below. forming a postcro-dorsal point on cach,

whereas the corresponding part of Cy. crassa

appears, in Baker's figure, to be smoothly

rounded and to run down to the telson as a

straight ftidge. Two other conspictious dif-

ferences are that the epistome is very much

shorter than broad (and different from that of

uny described species), and that the uropodal

exoped is relatively Jarge, plate-like, and

rejches to the end of the endopod in the ¢losed

position,

It seems clear that this is a new species, but

no sauistactory description can he given in the

absence of an adult male.

Group BURRANCHIATAE

Genus CERCEIS Milne Edwards, 1840

Cerceis aculicaudata (Haswell). Hansen, 1905:

127, Hale, 1929; 300. Nierstrasz, 1931:

214,

Sphaerama (9?) acuticaudata Haswell,

T8R1b; 197, pl 3, Fig. 9,

Localities: Vic. Griffith's Point, Port Phillip

(Haswell L&K1b); “This is a common

apectes” (Hale 1929), New record; Pearson

I. (R at 25 m, from algae on horizontal

face. R at 20-25 m).

Material: Three females (8.5-9.3 mm long),

all immature and Without ooslegites or

eggs.

Remarks: Specimens agree with descriptions

and figures of Cercels aeuticaydata except that

they lack the spines on the Urupods and the

spine on the pleotelson Is represented only by

a smooth median boss. Comparison with a

series of specimens from Western Port shows

that the growth of these spines is both allo-

metric and variuble.

Genus HASWELLIA Miers, 1884

Haswellia anomala (Haswell). Baker, (026:

273, pl, 48, figs, 8-9. Naylor, 1966; 192

Sphacroma (2?) anormnala Haswell, 188ba.

473, pl. 16, fig, 4,

Zuzara emarginata Haswell, 1881 b: 188,

pl. 3. fig. 5,

Taswellia emarginata (Haswell), Hansen

1905: 127. Hale, 1929: 304. fig. 304.

Localities: N_S.W.: Port Jackson (Haswell

188la): Vie.; Western Port (Haswell

L881b), Port Phillip (Naylor 1966); 8.

Aus! St. Vincent Gulf (Hale 1929). New

record: Pearson I. (R at 25 m).

Material; Seven females (5.88.6 mm long),

all immature and without eges, oostegites, or

modification of the mouthparts.

Remarks: The females of this. species are very

similar to those of Cerceis trispinosa. The uro-

poual exopods provide a convenient diagnostic

feature; in C. sispinasa females they are

longer than the endopods, while in A. anemate

they are both slightly shorter than the endo-

pods, and conspicuously toothed on the distal

edge. Comparison with a series of A. anomala

from Western Port confirms the identity of the

Pearson I. specimeus. The largest of them have

the hind. margin of the seventh thoracic tergite

produced in the centre (although not as fay as

in Haswell's figure of Sphacroma (7?) ana-

mala), a feature which supports Naylor's view

that S. (7?) anomala was the fernale of this

species and hence also supports his adoption of

the specific epithet anomala.

Haywellia cilicioides Baker, 1908: 158, pl. 10,

figs, (2-23. Hale, 1929: 304, fig. 305.

Localities: S, Aust; St. Vincent Gulf (Baker

1908, Hale 1929), New recerd: Pearson T-

(S at 30m).

Marerial: One adult male ( 9 mm long),

Remarks; The specimen agrecs with Baker's

(1908) and Hale's (1929) descriptions and

figures, except for slight differences in the

shape of the uropodal endopods, and in the

shape of the process of the Jast thoracic seg-

ment when viewed from above.

21>

Ww, F. SEED

Acknowledgements

Tam grateful to the Director of the Nationul

Muscum of Yictoria for facilities for this

study, und to the Science and Industry Endow-

ment Fund (C,S.1R,.0.) for a grant-in-aid.

Mrs. J. BE. Watson und Mr, A. Neboiss read

the draft manuscript and made a number of

helpful coniments.

References

Bagel, W. H, (1908), -Notes on some species of

the isopod family Sphaeromidae from the

South Ausiralian coast, Trans. R. Soc. 8.

Aust, 32, 138-162, pls. 3-10.

Baker, W. H, (1926).—Speciés of the isopod

family Sphaeromidae from eastern, southern

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Sac. S- Aust. 50, 247-279, pls. 38-53.

Bakrr, W. IT. (1928) —Australtan species of the

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Trans. R, Sov, §. Ads. 52, 49-6], pls. 1-6,

Barnarn, K. H. (19'4)—tConirihutions to the

Crustacean Fauna of South Affica, 3.—Addi-

tions. to the Marine Isopoda. with Notes on

some previously incompletely known Species.

Ann, S. Afr. Mus. 10, 32Sa—358a, 359-442.

pls, 27-38.

Hare. H. M, (1929).—"The Crustaceans of South

Australia”. Part 2, (Government Printer:

Adeluide: )

Hansen, H. J. (1905)—On. the Propagation,

Sirugture and Classification of the Family

Sphieromidae. Q. J] miarose, Sei, 49, 1s.

(193), 69-135, pl, 7,

HASwWeit, W. A. (1881a)—On some new Ans-

tralian Marine Jsopoda. Part I. Prac. Lite

Soe, NSW, 5, 470-481, pls. 16-19,

Haswrib, W. A. C€§88Ib)—Gn some new Aus-

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Sac, NSW. 6 181-196. pls, 3-4.

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tralian Stalke and Sessile-evyea Crustacea”.

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Hurry, D, E. (1961).—A Checklist and Key

to the Crustacea Isopoda of New Zealand

and the Subantarctic tslands. Trans. R_ Soe:

N.Z. (Zool.) 1(20), 259-292.

Teach. W, LE. (t&13-14).—Crustacenlogy. Jn

“Rdinhurgh REncyclopyedia* 7. (Blackwood

ve. al: Edinburgh.)

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naire des Sciences Naturelles” 12. (Levrault;

Paris.)

Munvins, R. J. (1962).—The Zoogeogranhy.

Ecology and Systematics of the Chilean

Murine Tsopods. Acra Univ. lind., NvF. Ava.

1, S7(11), 3-162.

Menzies, R. J... & PRANKENBERG. D. (1966).—

“Handhook on the Common Marine Isopod

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Miers, E, J. (1/884). -Crustaces. Jn “Report on

the Zoological Collections made in the Tndo-+

Pacific Ocean during the voyage of H.M,S,

‘AlerU, 1861-2," pp. 178-322. pls. {&-34.

(British Muséum (N. H,); London.)

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des Crustacés” 3. (Libraire Encyclopedique

de Boret: Paris.)

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1963. Isopoda, Afem. natn. Mus. View, 27,

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pls,

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‘Thetis’. Crustacea Part TI, Tsopoda Part Il."

(Australian Museum, Sydney.)

STRATIGRAPHY, STRUCTURE AND METAMORPHISM OF THE

KANMANTOO GROUP (CAMBRIAN) IN ITS TYPE SECTION EAST OF

TUNKALILLA BEACH, SOUTH AUSTRALIA

BY B, DAILY* AND A, R, MILNES}

Summary

DAILY, B., & MILNES, A. R. (1973). -Stratigraphy, structure and metamorphism of the

Kanmantoo Group (Cambrian) in its type section east of Tunkalilla Beach, South Australia. Trans.

R. Soc. S. Aust. 97(3), 213-242, 31 August, 1973.

An apparently conformable sequence of metaclastics forming the upper part of the type Kanmantoo

Group (Cambrian) has been mapped along 50 km of coastline between Tunkalilla Beach and

Middleton Beach.

Sporadically occurring black carbonaceous and sulphide-rich phyllites are confined to and

characterise the Brown Hill Sub-group. Associated immature "flysch-like"” metasediments were

deposited very rapidly in an actively subsiding basin by currents flowing mainly from the NW.

Numerous pebble beds, similar to those in the underlying Inman Hill Sub-group, reflect the

continuity of the Kangarooian Movements. The cross-bedded Middleton Sandstone at the top of the

overlying Wattaberri Sub-group was deposited by currents directed mainly towards the east.

STRATIGRAPHY, STRUCTURE AND METAMORPHISM OF THE KANMANTOO

GROUP (CAMBRIAN) IN ITS TYPE SECTION EAST OF TUNKALILLA BEACH,

SOUTH AUSTRALIA

by B. Daity* and A. R. MILNES}

Summary

Datry, B., & Mines, A, R. (1973).—Stratigraphy, structure and metamorphism of the Kan-

mantoo Group (Cambrian) in its iype section east of Tunkalilla Beach, South Australia.

Trans. R, Soc. 8. Aust. 97(3), 213-242, 31 August, 1973.

An apparently conformable. sequence of metaclastics forming the upper part of the type

Kanmantoo Group (Cambrian) has been mapped alone 450 km of coastline between Tunka-

lila Beach and Middleton Beach.

Sporadically occurring black carbonaccous and sulphide-rich phyijlites are confined to and

characterise the Brown Hill Sub-group. Associated immature “fiysch-like” mictasedimenty were

deposited very rapidly in on actively subsiding basin by currents flowing mainly from the

NW. Numerous pebble beds, similar ta those in the underlying Inman Hill Sub-group, reflect

the continuity of the Kangarooian Movernents, The cross-bedded Middleton Sandstone at the

top of the overlymg Wattaberri Sub-group was deposited by currents directed mainly towards

the east.

Kanmantoo Group rocks younger than the Middlcton Sandstone are unknown in the Mt.

Lofty Ranges, Because the formation is intruded by the Encounter Bay Granites, a thick

cover must have been present at the time of intrusion and metamiurphism.

Warm casts were the only fossils located in the study area und are suggestive of a marine

environment of deposition.

The sequence mapped forms the eastern limb of a regional anticline overturned towards

the NW. Two phases of folding are recognised. F; folds plunge shallowly towards the SSW

er NE. Eastwards from ihe core of the highly appressed and asymmetrical regional anti-

cline, F; folds in metasandstones become progressively more open, symmetrical and upright.

Mesoscale Fo folds with E. to SH plunges are confined to the eastern patt of the type section.

A weak crenulation of S$; is observable near Coolawang Creek, and becomes progressively

stronger towards the east.

The Encounter Bay Granites were intruded and had crystallised prior to the main phase

of FP, deformation because thin granite sheets, concordant with bedding, developed the §;

and S» schistosities during the folding episodes,

Stability fields for the observed metamorphic mineral assemblages show that the meta-

morphism of the Kanmantoo Group was effected at moderate temperatures (below 540°C)

and Tow pressurcs (below 3 kb). This is indicated also by the well preserved sedimentary

sftuctures found throughout this sequence of undalusite-staurolite prade rocks, Cordierite,

restricted to the proximity of the granite, records the highest grade of metamorphism within

the type section. Petrographic evidence suggesis that cordierite crystallised during the pre-

to early syn-Fy phase, a conclusion in harmony with the suggested pre-tectonic emplacement

of the Encounter Bay Granites. Petrographic evidence indicates that most of the sndalusite

formed during the late syn-F; phase of metamorphic crystallisation. In the post-F, and

pre-F. static phase of meftamarphic crystallisation, some andalusite, garnet, hornblende,

*Centre for Precambrian Research, Department of Geology and Mineralogy, University of

Adelaide, Adelaide, S, Aust. 3001,

+ GS.1R.0. Division of Soils, Glen Osmond, 5. Aust, 5064, Formerly, Department of Geology and

Mineralogy, University of Adclaide.

214 B. DAILY and A. R. MILNES

scapolite and chlorite grew across the S; schistosily, The 8. crenulaiion cleavage, where

developed, deformed porphyroblasts of this age. Albitisation postdates the Sw schistosity.

A peculiar “striped” layering. post-S; and pre-S. in age, occurs within the Petrel Cove

Formation west of Rosetta Head and resulted from alteration adjacent te tensional fractures.

Two distinc! groups of basic dykes. post S; and pre-S» in age. cut Kanmantoo Group

metasediments.

Introduction

A previous paper (Daily & Milnes 1971a)

discussed the geology of the Jowcr part of the

‘ype sezlion of the Kanmantoa Group (Sprigg

& Campana 1953) as found in the coastal clitls

of Fleurieu Peninsula between Campbell Creek

and the western end of Tunkalilla Beach (Figs.

1 & 2). The present paper gives the results of

our investigations of the geology for the re+

mainder of the type section east to Rosetta

Head near Victor Harbor. In addition, we have

extended our averse to include stratigraphi-

cally younger metasediments to the NE in the

Port Elliot and Middleton areas.

The stratigraphic succession und geological

structure over this 50 km of coustline (Figs,

3 & 4). differ significantly from that shown

on the map given by Madigan (1925), on the

Jervis (Campana & Wilson 1954) and Encoun-

ter (Crawford & Thomson 1959) 1;63,360

Carrickelnaa Hes

Normanwilie

Le]

555

Canneshaw

Afwadle Arver

KANGAROO ISLAND

Fig. LL

Figs, 2-4,

map sheets, on the BARKER 1:250,000 map

sheet (Thomson & Horwitz 1962) and in the

‘Handbook of South Australian Geology’

(Thomson 7m Parkin 1969). In essence we have

found that progressively younger formations

occur to the east despite the advent of folds

which repeat parts of the sequence. These: folds

dre inclined to upright and plunge at relatively

low angles towards the SSW. hut as shown on

the maps, some exceptions in plunge direction

do occur, particularly in connection with parts

of the Wattaberri Sub-group.

Our main aims in studying the geology of

the type Kanmantoo Group have been to te-

assess. US stratigraphy and age limits and to

try and determine the relative time of emplace-

ment of the Encounter Bay Granites in con-

trast to the isotopic ages obtained by Dasch

ef al, (197), In the presumed absence of diag-

nostic foszils within the type section, we have

Houghton =

> ex

ADELAIDE a

ao e uneaa

Naifne e Brukungea

\ « Kanmantoo

I Call +45,

oc Sa, 2 Callington

tr Barber C4

Selick Hil A eo Wit Cornpass

cut Hil

ee a)

got alaman HiRes

ue Hindmarsh Valley

Ass,

“SA

DUDLEY’ FEMINSLULA,

~G Willoughby

20 K'LOMETRES

bent el ee I

Locality mup of geographic features. exclusive of those shown on the geological maps in

GEOLOGY OF TYPE SECTION, KANMANTO0 GROUP (CAMBRIAN) ON

been forced to define the relative age of this

emplacement i tetms of the structural and

metamorphic history of the Kanmantoo Group,

Fortunately, sufficient rock samples were col-

lected and enough structural observations were

recorded during our traverse jo enable us to

siggest the emplacement of the granites prior

to the culmination of the first phase of defor-

mation.

We have not attempted a rigorous analysis of

the structure and metamorphism of the Kan-

manloo Group it tly Lype section, and further

work to this end is warranted, However, oite

of us (Milnes unpub.) has discussed “The En-

counter Bay Granites and their enviranment’ in

greece delail in a Ph.D, thesis, aubmitted to

the University of Adelaide.

Stratigraphy

In presenting the geology of the upper part

of the Kanmantoo Group we have revised the

stratigraphic terminology previously applied in

the type section (Daily & Milnes 19729). This

scheme is given in Table {, As explained in

the 1972 pauper, we have discarded the term

TABLE. |

Stratigraphic scheme for the Kanmantoa Group tn

ity mpe section between Campbell Creek anil

Rosetta Head. The table also includes strotigra-

phicaily younger metasediments ia the Port Eltiot-

Middteion arva and alsa shows the relationship

af the Kanmanioo Group ta-elder rocks (Precam-

brian and Cambilan) on Fleurieu Peninsula, The

regional unconformity between Precambrian and

Cambrian strata represents roughly the stratigra-

phie interval from the ABC Quartzite of the Flin-

ders Ranges to the hase of the iransgressive Carm-

brian sleposits-

Middiciwn Sandstone

Waraherel

Sub-group

Petre! Core Formation

Belauhidder Farmaion

Town Flu

Snb-eroun

Tunkalilla Formation

Tapanaiiya Farmition

KWanmanion Grain

Talisker Cale-siltsnone

Cambrian Sysivii\

Tamz2c Hill

Sub-aroun

Wacksiairs Passage Formation

Cavitkalinga

Alvad

Foviation

Campana Creek Mumher

Biiwhnte Crock Sillfione Member

Madigan Inlet Meniber

Normunyvilte Group

Remonal Unheonlinity

Marinn Group (Laie Preegnibrignl

Brukunga Formation but have retained the veo.

graphic terms Inman Hill and Brown Hill to

qualify sub-proup names, This procedyre re-

tains the position of the boundary between the

Taman Hill Formation and Brown Hill Beits

as desigaated initially by Forbes (1957), More-

over, the base of the Brown Hill Sub-group,

which is easily recognised, docs not correspond

to the base of the Nairne Pyrite Member at

the hase of the type Brukunga Formation. The

base of the Brown Hill Sub-group is estimated

In be 3000-4000 m above that position in the

Nairse region where the Brukunga Fornsation

was originally detined,

The following abbreviated gocount has been

made from our field notes of the coastal sec-

tions and environs east of Tunkalillu Beach

A. INMAN HILe Sup-croup (new rank)

The Inman Hill Sub-group (Table 1) con-

tains the Backsteirs Passage Formation,

Talisker Crilc-siltstone and Tupanappa Forma-

tion, All three formations occur in superposi-

tion in their type sections. In addition, we have

now located them on Dudley Peninsula, Kan-

guroo 1. (Daily & Milnes 1971b) where they

appear to be of identical facies. However, we

have had difficulties in identifying the Tapa-

nappa Formation in the northern sections of

Fleurieu Peninsula, although Tapanippa For-

mation of comparable lithology to that ex-

posed in the type section is well exposed along

the Mount Barker Creek, near Callington, fur-

ther to the north. So far we have not mapped

any intettongucing relationships between typical

Tapanappa Formation and other formations,

nor have we recognised fault relationships that

Might account for jis apparent absence in some

sections, Nevertheless, we believe that such

possibilities do occur and we have recently

undertaken investigations in key areas to solve

these problems,

Tapanappa Fermation

Detailed observations on the lower part of

the Kanmantoo Group (Daily & Milnes 19714),

ditt not extend beyond the western end of

Tunkalilla Beach where the modem coastal

clifis abut upon the beach, However. there ix

an arcuate line of old coustal cliffs behind an

alluvial bench backing that beach which per-

Mitted collection of data for the uppermost part

of the Tapanappa Forniatiun, despite the rela-

tively poor outereps in comparison with those

in the thodern coastal cliffline, The sequence

Cunsisty of dark coloured, thick-bedded to

laminated, generally fine- to coarse-grained

metusandstoncs, although near the top of the

formation ver¥ fine-grained metasandstones

predominate. The individual metasundstone

beds, rarely more than 1 nm thick, are split by

povrly eutcropping and {frequently Juminated

octasiltslones and phyllite interbeds which are

penerully much thinner than (he metasand-

stones, These pelites range down tu partings of

i few millimetres. Poorly outcropping intervals.

many in excess of 10 m Stratgeaphic thickness,

are presumed metasiitstones or phyllite beds.

Bunds und tods ol cale-silicates occur spora-

divally in the metasandstones and even in some

of the finer grained lithologies. Porphyroblasts

oft chiurite. muscovite and bielite dre common

in the finer grained lithulogies, especially the

phyllites, ws well as some of the metasandstone

bands. Onternps of small-scale conglomerates

uceur ws thin discontinuous bands in same uf

the coarser grained metasandstones but their

presence in the sequence was generally inult-

cated by float rather dha outcrop,

B, Brown Hit. Sup-croue (new rank)

The base of the Brown Hill Sub-group and

the Tunkalill Pormatioi is marked by a

sequence of dark blue to black laminated phyl-

lites ybout 15 m thick (not 10 m as in Daily &

Milnes 197 1a, p, 207), and outcrops on a small

suddle hehind the beach about 2.5 km west

of Tunk Head. The Tunkalilla Formation to-

gether with the overlying Balquhidder Forma-

tion constitute the Brown Hill Sub-group. ‘The

lithologies within the sub-group ure not unlike

those found in the Tapanappa Formation and

indeed jt is impossible to: assign limited se-

quences to either unless the dark blue-black

carbonaccous and sulphide-rich phyllites cha-

racteristic of the Brown Hill Sub-group. are

located within them. Fortunately, dark

coloured phyllites of this type are unknown to

us guiside the sub-group within the type ares.

Geopraphicolly, they ure quite extensive as they

are known from Middle River (upstream from

the dam site} on Kanyguroo L, liorth to at least

ihe Callington areca in the eastern Mt. Lofty

Ranges.

Tunkalilla Formation (new name}

Vhe dark coloured laminated phyllites rark-

ing the base of this formation conformably

overlie the Tupanappa Formation metiasédi-

ments, When weathered, the phyllites are

characteristically stained yellow and brown by

jarosite ond guethite due to the oxidation of

iron sulphides within the Tock, Stratigraphically

above this basal unit are about 30 m of poorly

cutcropping dark coloured medium- to course-

grained mactusandistones with interbedded meta-

B. DAILY and A. R, MILNES

siltslunes und phyllites. Succeeding this there is

a khaki to mid-grey coloured phyllite about

30 m thick overlain by a 200 m thick sequence

of alternating Lo m thick bands of fine- to

mediuin-zrained melasandstones und Khakl to

mid-grey coloured phyllites. ‘These are in turn

overlain by a thick sequence (ahoul 150) a}

of predominantly well laminated metusiltstones

(Fig. 8) andl phyllites with minor metusand-

stone interbeds cut-and-fill into the finer clas-

tics, This interval vecupies: low ground and

outcrops poorly. Elongate to ovoid porphyro-

blasts wf micas iunlchlorite are Cummon in the

metasiltstones. Several small quartz-feldspar-

chlorite-muscovile pegmultiluy oocur in silky

phyllites near the mouth of Tunkalilla Creck.

A well developed crenulutvon is present in the

phyllites immediatcly adjacent to these ‘sweat’

Peymaliles, but this is local and has nov been

vbserved elsewhere.

The topmost part of the Formation is a well

laminated phyillite-metasilistone to fine-grained

metasandstone sequence capped by sc least 3 m

of blue-black luminsted carbanuccous phyllites

in which the alteration of sulphides. has. pra-

duced jurosite and poethite. Cubie shaped voids

after pyrite are readily upparent in the wea-

thered phyllites. The best outerops can be in-

spected high up on a mainly soil-covered west

facing cliff about 100 m east Of Tunkalilla

Creck, after which the formation is named.

The position of the upper boundary of the

Tunkalilla Formation is plotted on ihe geo-

Jogical map (Fig. 3). In the first creek west of

Cullawonga Creek. a & m thick band of black

sulphide-rich finely laminated phyllites stained

With jarosile and geethite marks the top of the

formation, It is underlain by about 3 m uf

metasinistone., Below the melasandstune there

is a much thicker poorly outcropping bund of

blue-black carbonaceous and — sulphide-rich

phyllites which, providing there are no struc-

(ural complicahions, may haye a thickness of

30 m. Paler coloured phyllites and metasilt-

stones occur below this. We may have missed

this approximately 30 m band of black phyllite

in the type section due lo thick soil gover at

this stratigraphic level. In craverses east of Cul-

lawonga Creek however, we Jocated only the

upper of the tWo bands and therefore i is more

Jikely that this thick band is a local develop-

ment.

The only fossils found within the formation

dre abundant worm casts in outcrops of sand-

blasted metasandstenes at the back of Bolla-

parudd’a Keach, adjacent ba the westeen hank

GEOLOGY DF TYPE SECTION, KANMANTOAO GROUP (CAMBRIAN) ZL

of that creek, The worm easts (Figs. 9 & 14))

are exceptionally well-preserved despite the tec

tonisia and metamorphism. ‘They are weathered

out in full relicE in an ourgrop about 8 m tong

and their tubular and sinuous nature can be

seen to pericction, particularly in sections nor-

mal to the bedding. The bioturhared interval,

Which is obour 20 cm thick, forms the topmost

bed in a large scour-channel (Fig. 14). The

lower parts of the channel comtain shale-chip

conglomerates in which the now phyilite frag-

mcals are scattered in a metasandstone matox.

Thus the Tunkolilla Formation in its type

section ut Tynkalilla Creck is a sequence (at

levtst 250 mM thick) of muinly fine-grained clas-

tics whose base and top are marked by bluc-

black carbonaceous and sulphide-bearing Jami-

nated phyllites of « characteristic appearance,

In the region to the narth of Hindmarsh Valley

mapped tty Forbes (1957), 4 seemingly iden-

tical sequence can be found on Mr, J. Grevn's

property just over | km SE of *Panybuly”

homestead (see Milang 1:43,000 map sheet,

Horwitz, & Thomson 1960, fo) the geographic

position of “Pambula''),

Balquhidder Formation (new name)

This formation is named afler the property

known as “Balquhidder (see Fig. 3), Its lype

section spans the coastline from a puint

approximately 2 km west of Tunk Head ease

te a point about 0.7 km west of King Poine,

where the much finer grained metaclastics

marking the base of the overlying Wattaberri

Sub-group are first encountered. There is con-

tinlOus Outcrop over this upproximately 30 km

of coastline except for the two stretches occu-

pied by Parsons Beach and Waitpinga Beach

However, the sequence is repeated by folding

across these two intervals so that our observa-

tions have covered most, if not all, stratigraphic

Jevels within the formation. The oldest part of

the formation occurs within a southerly-phing-

ing broad synclinal structure whose axis les

immediately west of Tunk Heath

A sequence of medium- to coarse-grained

metasandstones with metasiltstone interbeds

vecurs at the base of the formation, These are

conformable with the underlying Tunkalilla

Formation, About 300 m straligraphically

above the base of the formation and west of

Tunk Head. there is a 10 m thick sequence of

black carbonaceous and sulphide-rich phyllites,

Exposures are normally covered by sand on the

coast between this outcrop and the base of the

formation, but a seyvenge can be examined ine

land in the ancient coastal cliffs. The bulk of

the rocks are thick-bedded, medium- to coarse-

gramed metasandstones with thin interbeds of

metasiltstones or phyllites, However, there ure

intervals Where the metusilistones (up to 3 im

thick) are the dominant lithology and are inter-

bedded with metasandstones up jo | m thick.

Some thin blue-black carbonaceous and pyritic

phyllites were also nuted, Porphyroblasts of

chlorite and micas occur in many phyllite inter-

beds as well as in some fine-grained metasand-

stones.

The basal part of the formation is best seen

it coustal exposures, for example in a traverse

from Tunk Head east to Bollaparuilda Beach.

In these superior outerops the sequence has a

different character, For instance, many of the

seemingly massive metasandstones are well

laminated and crass-bedding becomes nore

apparent. Other notuble features include phyl-

lite-chip conglomerates (up ta 0,5 m thick)

which are associated with coarse-grained to

zranule-rich metasandstones in cut-and-fill

structures, load casts and associated flame

siructures, and beds with climbing ripples

(Figs. 11-13). Cale-silicute rods and hands are

also apparent (Piys. 15 & 14),

Above the lowest blue-black carboouceots

and sulphide-rich phyllites within the Balyu-

hidder Formation on both limhs of the Tunk

Head synclinc, medium- ta yery coarse-grained

missive anu laminated mectasandstones are do-

minant (Figs 17-19). The beds are variable in

thicknesa and generally less than | m_ thick,

ancl where this is the case the sequence has

somewhar flagey appearance (Fig. 20). How-

ever, there are intervals where metasandstones

are Up to 3m thick. Nevertheless, the thickest

bed recorded was. a 15 m thick band of

medium- to coarse-grained metasandstene

occurring adjacent to a thin black carbonaceous

and sulphide-rich phyllite within the uppermost

beds of the syncline, Thin bands and lenses of

small-scale pebble conglomerates and phyllite

chip bands occur sporadically through the

sequence and are generally associated with the

coarser sand mteryals. Small-scale sedimentary

structures are most frequently found in the

metasillstones and laminated phyllitic intervals

(Fig 21). Cale-silicate bands ad rods are

again common.

The black ¢arbonaceous snd sulphide-rich

phyllites are best seen on the eastern limb of

the syncline just vast of Tunk Head with the

highest band visible in a gulch immediately

west of the tazor-edged ridge constituting that

head, Sulphides concenrewied into cross-culting

218 fh. DAILY and A, R, MILNES

veins within this wnit at thiy focality were pro-

byhly remobilized at or subsequent to the ume

of metamorphism (Vig. 22).

Between Calluwonga and Bollaparudda

Beuches, the hagal part of the formatiun ts simi-

lar tw that described above, except that small-

scule Conglumetutes are present in some of the

cut-and-fill structures within thick mietasand-

stones. Phyllite-chip conglomerates are again

conimun ussaciales.

On the point 0.4 km SE of Bollaparudda

Beach, there are massive and well-bedded

course-grained metasandstanes, 15 em to 7 om

in thickness. ulternating with phyllite and meta-

siltstoie interheds. Many sands are bioturbated.

Higher in the sequence pebble bands (includ-

ing gaciss pebbles up to S cm across) and

lenses of small-scale conglomerates occur with-

in laminated medium- to coarse-grained: meta-

sandswnes (Fig, 231. Phyllite-chip congle-

merutes ure aussaciuted with these canglomer-

ates venerally near the bottom of chunnoels.

Additional pebble bands in very massive lonk-

ing mielasanustones occur higher im the 3e-

quence. At first sight some thick bands appear

lo be structureless graded units with pebbles

near the base and. with grain size fining up-

wards, However, in all cases the sands were

found in detail to be well bedded (Fig. 24).

The high incidence of conglomerates in the

lower purt of the formation cast of Bolla-

purudda Beach contrasts with their relative

paucity further west. The conglomerates arc

comparable with those found in the Tapanappa

Formation. Similar conglomerates in’ rocks

which we regard ay being well down in the

Balquhidder Formatiun occur in the Cut Hill

roud-eutting: on the Mt. Compuss-Victor Har-

bor toad. ‘Therefore, it seems thal conglome-

rates in this general stratigraphic position may

be a widespread feature of the formation, thus

refiecting the continuity of the Kangarooian

Movements (Duily & Forbes 1969: Daily &

Milnes 1971a) which were partly responsible

tor the deposition of the Kanmantog Group.

A byck carbonaceous and sulphide-rich

phyllite occurs near the cape about 1 km cist

of Bollaparudda Beach and is overlain by a

seyuience of anrinated to poorly-bedded meti-

sandstone beds {up to | om thick) with thin

phyllite and metasiltsione interbeds. From here

to the mouth of Coolawong Creck the strike is

almost parallel to the coast. A 3 m thick band

of black carbonaccous and sulphide-rich phyl-

fite overlain by thick poorly-hedded metasand-

stones and thin {nterbeds ol metasiltstanes and

khaki-coloured phylites occurs at the moulll of

Coolawany Creck This may be the same sel.

phide band 4s seen on the cape alluded to

above.

Between Covlywang Creek and Pitsons

Beach, a number of fuld hinges and minar

sults were loculed within the successiun. Mak-

ing due allawance for these, the sequence 's

seen to consist mainly of orassive Lo yell-

laminated metasandstones in the lower part of

the succession. Many of the channels cut within

the sands are filled with coulse-graincd to

granule-sized claslics including, Jenses ol sill

pebbles, Nodules aiid irregular shaped bands of

chle-silicate lithology are developed in some

parts of the sequence. About T kim east of

Coolawang Creck, porphyroblusts of scapolite

occur in slumped and laminated metasand-

stones and phyllites, [a some of the metasill-

stones hoth scupolite and garnet muy be found

In ihe sume arca pexmatites and feldspathived

vones are common and are offen associated

with tensional Features developed in) massive

metasandstone bedy split by thin phyllites ( Figs.

35 & 26). A litle higher in the sequence some

of the mussive metagandstones (1-2 m thick

sod split by phyllites up to 1 m thick) are

biolurhuted towards their tops. A weak créenu-

lation cleavage, noticed for the first lime in our

travetse, becomes much more apparent as one

moves to the east. und provides evidence for a

second phase of folding, The first-generation

folds are open and asymmetric with steep

westerly-dipping unticlinal limbs in contrast to

the inclined folds further west possessing over-

turned easterly-dipping anticlinal limbs, The

opening up of the fold hinges might he con-

sidered a function of distance wway from the

crystalline basement at the time of folding.

lhe remainder of the sequence vast to Par-

sons Beach is made up of flaggy laminated

metusandstones, generally less. than 1 m thick,

with interbedded thin laminuled and sumetimes

rippled metasiltsiones (Fig. 27) and ercnulated

phyllites up fo 0,6 m thick. Some of the sanils

are biowrbated und some contain cule-silicate

nodules, A feature of this pant of the formation

is the Fashion in which the cleavage has des-

troyed or vastly modilied the fine sedimentary

structures within the top (and bottom) few

centimetres of the sandier beds. Bedding sur-

faces, <imilar to thi shown in Fig. 19, show an

obvious lineation along the cleayage/ bedding

intersection duc to the smearing out of the sedi-

mentary siructures, Another expressiun of the

cleavaye/ bedding intersection 7s the pro-

GROLOGY GF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN)

nounced ridge-and-furrow Tinention seen on

the base of some metasandstones (Fig, 28)

This simulates the cast of 4 glaciated pavement

ur sedimentary gfoove casts.

‘Yhe readily accessible sequence farming the

headland hetween Pyrsums Beaeh and Wait-

pings Beach is on the castern limb of a SW

plunging syncline occupied by Parsons Beach.

Massive und laminated coarse- to fine-grained

metasandstones with interbedded metusiltstones

und phyllites again constitute the succession.

In general, the metayandstone bunds increase in

thickness up the sequenee and near Parsons

Beach some beds pre nearly 6 m thick. Sedi-

mentary structures such as cross-bedding

faceasional sats up to 0,65 m), plunar-hedding,

slumping, convolute-bedding (Fig, 29), lond

gasts and jssociated Name siriictures, current

ripples, simple and compasite cut-and-fill struc-

tures {these are sometimes associated with thin

small-scale conglomerates und phyllite-chip

conglomerates), and bioturbated sandy inler-

vals were recorded. There wre several thick

phyllite and metasiltstone intervals. particularly

towards the bottom of the exposed sequence.

Some of these phyllites are crenulated and con-

tain cordierite and other porphyroablasts. Cale-

silicate bands. and rods, some of which are at

least 2 m long, are prominent through many of

the metasandstone intervals, Segregations pos-

sessing the sume mineralogy and encompassing

parts of pebble beds were also recorded.

There is a total absence of Kanmantoo

Group rocks across the 4 km wide sanily

Waitpinga Beach, Cainozeic und Permian

depusits (uncoliuured in Figs. 3 & 4) blanket

these rocks for many kilometres inland. How-

ever, the seyuence is continued uninterruptedly

along the coastline from just west of Newlund

Head to the vicinity of Rosetta Head.

On the western side of Newland Head there

ure very thick (up to 10m) medium- 19 coarse-

ernined metasandstones with pebble bands

which are mainly assuciated with out-and-fill

structures. The sands are well laminated and

cross-bedded within and away from the channel

hottams (Fig. 3M). Pebbles are scattered

through some of the hedded metasindstones

ind in One instance were seen to be present a>

the stoss side but absent on the lee side of

mego-ripples. A band of ceenulated andalusite

schist was found about 20 m east Trom the

commencement of oimcrop. Above this and

below a 2 mihick black carhonaceous anid sul-

phide-rich phvilife is a thick metasandstonc:

219

Stratigraphically higher ts a very thick sequence

of metasandstones (beds generally Jess than

2 m thick) which alternate with phyllites or

Thetysiltstones. ang an ocexsional much thicker

Metusandstone interval (Fig. 31), Two addi-

tioagl Black carbonaceous and sulphide-bearing

phyllites and two bands of andalusile schists

were located in this latter sequence, Strati-

stiuphically above and perhaps 300 m NE of

Newland Ueud, another prominent blue-black

curbonuceous and sulphide-rich phyllite is inter

bedded in the flaggy sequence (Fig. 32). This

can be readily followed for about J km before

it strikes jwland and is Jost from view. IL is

overlain by coarse metasandstones containing

weak developments of small-scale couglomer-

ales in an otherwise flaggy sequence, From this

point onwards to within about 2 km west of

King Point (Fig. 32), the strike of the beds

parallels or is slightly oblique to the precipitous

coastline, parts of which ure totally inacces-

sible. Consequently, our traverse was made

mainly along the tep of the coustal cliffs. An-

other slightly younger blue-black phyilite

occurs 2.4 km NE of Newland Hew and below

well-bedded, coarse-grained. impure metasand-

stones. split hy thin phyllites.

Aboul 1,5 kin WSW of King Beach a 2m

thick band of a comparable hlie-hlack sul-

phide-rich phyllite uceurs above a regnlarty

bedded medium- to coarse-zrained metasand-

stone with thick laminated phyllite partings, Tt

is either stratigtaphically above or possibly on

the same horizon as the blue-black phyllite

mentioned shove. Towards King Point lami-

nated metasandstones, often with cut-and-fill

structures, occur in beds varying from abeut

19 cm to § m in thickness. Banded metsilt-

stones aud finely crenulated phyllites (maxi-

mum thickness about 2 m1) occur as interberls

and may contain porphyroblasis of mica or

more rarely andalusite.

The uppermost part of the formation is

marked hy a sequence of relatively fiagay

metasandstones and tactasiltstumes, in which

there are a number of interbeds of knotted

undulusite schists, Cordicrite parphyrnblasts

andl =o quartz-tich uyyregites co-exist. with

undulusite in some of the schists (Fra, 347, ‘the

cordicrite porptyroblasts and quact¢-rich agere-

gales ute deformed in the plane o£ the pro-

minent mica schistosity (S,) resulting in the

development of small augen. Tn many pelitic

units a prominent discontinuous layering occurs

parallel to S, defined by the alignment of these

augen. Andulusile porphyroblasts. which are

22)

seen in thin section to postdate the augen

development, also help to define this layering.

Andalosite-rich pegmatites containing mus-

rovite and corundum occur within this interval,

Small-scale first- and second-generalion folds

ate commonly present m the metasediments

vdjioent to the pezmiatites, which are invariably

strongly boudinaged,

C WATTABERRI SuB-GROUP (new name)

A marked change in sedimentation took

pluce ufter the ueposition ef ihe Balquhidder

Fornilion duc to the influx of fine-grained

ctustics. These now constitute a sequence of

essenlially phyllites or schists, metasiltstones

und fine-grained metasandstones and are dis-

cussed below under the name of Petrel Cove

Formation, The succeeding characteristically

faminuted and cross-hedded Middleton Sanu.

Stone is Yrouped with the Petrel Cove Forma-

lion 45 the Wattaberri Sub-group. named from

the property called “Wattabers”. some 2.5 km

northeaf Port Elliot.

Perrel Cove Formation (new name)

This formution is much less resistant to ero-

sion than the Balquhidder Formation and thus

forms | more subdued topography, [t occurs

in low ¢lill lines between a point 0.75 km west

of King Beach and Petrel Cove. aftee which

the formation is named. Good outcrops can

also be inspected at low tide in Rosetta Huar-

boron the NW side of Rosetta Head. All parts

of the formation in this area are readily

accessible. It can be regarded as one of the

key areus in the State where so many aspects

of the effects of metamorphism and tectonism

of a sedimentary sequence can be demunstrated

clearly. All efforts should be made to preserve

this stretch of coastline as a geological monu-

Hent. Vanous aspects of the geotory of parts

of the sequence have already been discussed by

Browne (1920). Bowes (1954), Hobbs & Tal-

bor (14956) and Talbot & Hobbs (1968 and

TV69],

A sequence of folded porphyroblastic and

sindalusite-cordierite schists constitutes the hase

of the Petrel Cove Formation. These confor-

mably overlie the topmost unit of the Balqu-

hidder Formution which 1s composed of a

sequence of fine-grained metisandstones and

mejasiltytones, The schists exhibit a well-

developed gugen layering (S,) axial plane to

F, tolds. which are cleatly outlined by the

hedding (S\,) ws is seen in Figs. 35 and 36, Tn

the saihe Oulerops (ste especially Fig, 35) verv

thin light-coloured layers pervade the schists

and appea as a senes of thin closely spaced

B. DAILY and A. R. MILNES

stripes (S,) at a low ongle to the auger layer-

ing. These stripes define what is herein termed

a “striped” layering (see also Talbot & Hehbs,

1968), We regurd this “striped” layering as

having developed by alteration along tensional

(ractures post-dating the F, folds. Note also

that tn the same outcrop (Fig, 35) there arc

“pincth-and-swell” pegmatitic layers parallel io

the “striped” Jaycring and along which disloca-

tion hus taken place, In several areas more than

one set of “striped” layering can be recognised.

A well laminated metasilistone sequence

(Fig. 37). parts of which are strongly folded,

oecurs on the wave-cut platform pbove the

basal anulalusite-cordierite schists, Mics porphy-

roblasts, light-coloured augen m S,, and an in-

frequent “striped” layering show up in parts

of this succession. Dislocation of bedding paral-

lel to the stripes is ugain evident in some aul-

craps.. Stratigraphically above are porphyro-

blastic metasiltstones and schists with intervuls

Showing either isolated augen in S, or with

dugen sufficiently concentrated to produce an

augen layering in S;. Very fine-grained meta-

sandstones are interbedded with these. On King

Point the beds are well laminated and exhibit

small-scale sedimentary structures (Fig, 38).

Near this locality some calc-silicate layers occur

parallel to the bedding and shaw « cleavage/

bedding intersection plunging towards the

south, These beds strike across the bay rowards

Petre] Cove,

Along the coast between King Beach and the

contact hetween the Petrel Cove Formation

with the Encounter Bay Granites on Rosetta

Head, the incompetent metasediments within

the Petrel Cove Formation show numerous

meso-scule Folds of two generations, The folded

sequence consists of very fine grained meta-

sanistones with interbeds of metasiltstones and

crenulaled schists. Numerous deformed sepli-

mentary structures such us those in Pigs, 39

and 40 are common. Similar sedimentary struc-

tures have been figured or discussed by Hobbs

& Talbot (1966) and Talbot & Hobbs (1969),

The common occurrence of “striped” Llayer-

ing (Figs. 39-47) which, in a thick homo-

geneous rack type, could passibly be mistaken

for bedding has heen mentioned above. This

layering is markedly refracted across the

boundaries between the metisandstones and the

andalusite-cordierité schists. The layering is not

only discontinuous hut may even show a

feathering effect fPig. 454, aguin u feature sug-

gesting that rt developed in response to ten-

sion. In addition, it formed afler the F, feld-

GEOLOGY OF TYPE SECTION, KANMANTOO GROEP ICAMARIAN) 32]

ing phuse because faint stripes cut straight

through strictures on the tap of heds deformed

by that phase of folding (Fig. 39). In many

andalusite-cordierite schist intervuls, especinlly

along the coastline immediately west of Petrel

Cove, the “striped” lavering has been folded

on a amall scale about an axial plane purallel

10 the crenululion cleavage (S.) (Figs, 43 and

461. Many of these andalusite-cordicrite schists

show either a preferred concentralion ur a

depletion of andalusite porphyroblasts paraile}

to the “striped” layering (Fig. 47),

Cummozoic and Permian sediments (un-

colonred in Fig, 4) blanket mast of the region

between Rosetta Head and the hills lying to the

nerth of Port Elliot. Over this distance no rocks

helonging to the Wattaberri Sub-group are

known to Getcrop on the coast, However, in a

section between Brown Hill and Wattaberri

we have inferred a houndary heltween the Bal-

qguhidder Formation (containing some blue-

black carbonaceous and pyritic phyllites) and

an overlying dominantly phyllitic-metasiltstone

sequence identified as the Petrel Cove Farma-

tion (Fig. 48). Despile a prolonged search in

the area, we have been unable to locate anda-

lusite or other distinctive melamornphic

minerals so characteristic of many parts of the

formation in its type section between King

Tomt and Rosetta Head. Stratigraphically

above these racks are metasandstones of w dis-

unetive facres which we call the Middleton

Sandstone. This formation is best examined in

the Middleton quarry and on Middicton Beach

Metasandstones of an identical facies and

stratigraphic position lie in contact “ith the

Encounter Bay Granites on the eastern end of

Kangarcur 1,

We have been unable to locate a contact

between the Petrel Cove Formation and the

Middleton Sandstone une ta imperfect qutcrop

Nevertheless, 9 tentative houndary has been

positioned as shown in Fig, 4. Rocks shown as

Middleton Sandstone pre characterised hy the

presence of epidote-rich bands.

Middleton Sanestane (new name}

The best section of Middleton Sandstone is

seen on the wave-eut platform in the vicinity

of Middleton (Pig. 4). These outcrops. which

are totally isolated from other Kunmantoo

Group rocks, consist largely of grey-coloured

fine-prained metasandstones which are gener-

wily Ughter in colour and mure quartzese than

the bulk of the metasandstones found in the

Kinmunton Group, with ie exception of some

of the Inmun Hill Sub-group metasandstones,,

for example those of the Backstairs Passage

Formation, The metasandstones ure typically

very well-laminated and are commonly cross-

bedded wilh sets up to 1.2 m thick (Fig. 49)

and with an indicated current direction gener-

ally from the west throughout much of the

sequence. In some of the higher parts of the

outcropping sequence, more random current

directions are indicated, Some slumping down

the direction uf the cross-hedding is evident.

Breaking the monotony of thie well-laminated

sequence ure intervals with minor sedimentary

structures. mainly small-scale current ripples,

which include some starved ripples involving

material of somewhat different grain size.

There wre also rare metasandstone feds up lo

0.5 m thick containing angular pbyllitice clasts

up ta 30 em long and 15 cm thick, though

generally the clasts are platy and less than 5 cm

acress, They represent the ripping up of partly-

indurated mudstones by strong currents and

their subsequent depositinn in scour-channels

after very limited twansport. The only other

metasediments present are a Few metasiltstones,

up wo 10 m thick, containing chlorite and

actinolite,

One of the mast conspicuous features of the

sequence is the prevalence of pale-green

epidote-rich sepreeations which are developed

consistently throughout the succession,

Albitised bleached zones of alteration ate also

presence. Most of the epidote-tich segregalions

vecur eilher in bands or as lenticular patches

and nodules parallel to the bedding (Figs. 50-

S52) but some epidole occurs in association with

quartz-chlovite-feldspar pegmatites that are de-

veloped in fractures and boudinaged zanes

All beds in the sequence fuce north. Obser-

witions show that the frequent occurrence of

overturned southerly dipping beds is due solely

jo warping locally developed along the sirike.

Practute-cleavage/ bedding intersections indi-

cute that the heds belong to the southern lind

of a synelinc plunging shallowly towards the

east, This syneline is a second-generation fold

as Shown by overprinting relationships in

Midd'eton Sandstone in the Middleton qitirry

The recognition of Jarge second-generation

folds in this area significantly adds fo the small

number of macroscopic F., folds reparted fror

elyewhere within the Mr. Lofty Ranges hy

Offler & Fleming (1968),

No upper boundary to the Middleton Sand

stone is known on the Fleurieu Peninsula, and

consequently this formation comprises the

youngest Kanmanino Group rocks in the

322 B. DAILY and A. R. MILNES

eastern Mt. Lofty Ranges. Because the En-

counter Bay Granites exposed at Port Elliot

seem to have intruded rocks of this formation,

a substantial sedimentary cover must have

existed above the Middleton Sandstone at the

tine of granite emplacement and metamar-

phism. This cover is likely to have embraced

rocks ef Middle Cambrian to possibly Karly

Ordovician age, as rocks spanning this sugaes-

teil lime interval occur on Yorke Peoinsula

(Datly 1969) and in the Flinders Ranges

(Daily & Forhes 1969).

D. INTRUSIVE Basic Dykes

Two groups of basic dykes that have in-

(ruded the Kanmuntoo Group within the type

section wre shown in Figs, 2-4, The dykes of

the first group are transgressive fine- to

meditim-grained metadolerites, Similar rocks

have intruded the Encounter Bay Granites at

Rosetta Head and Port Elliot.

‘The second group consists of hasic dykes

exlensively contaminated by meta-sedimentary

rock material. One such dyke containing large

feldspar megacrysts. intrudes Balquhidder For-

mation metaxediments along the coast cast of

Tunk Head (Fig. 3). This dyke was described

by Madigan (1925), A second contaminated

husie dyke-rock occurs in the line of ancient

coustul cliffs backing Tunkatilla Beach, but it

is poorly exposed. Sirnilar contaminated basic

dykes have intruded the Middicton Sandstone

dong the south cous: of Dudley Peninsula

(Kingarco I), west of Cape Hart. The results

of our investigations of (hese rack lypes will be

presented tna subsequent communication.

Structure

A lar Structruse of He Mera-sepimMen-

TARY SEQUENCE

An Interpretation of the geological structure

of the Lower Cambrian rocks exposed alone

the south coast of Fleuricu Peninsula between

Campbell Creek and ‘Tunkallly Beach has been

even in Daily & Milnes (1971a). This

sequence. involving the upper parts of the Nor.

manville Group’ and the lower parts of the

Kanmantog Group, is contained within a NE

plunging regional anticlinal structure which is

overturned io the NW [Fig. 2}. On the normal

eastern limb of this fold between Madigan fn-

let aud Tunkalilla Beach, all the mapped

mucroseale folds are believed to be first-

generation (F,) structures, Generally they

conform to the style of the regional fold, and

indeed to the style of folds developed in the

Late Precambrian ‘lorrens Group rocks in the

Houghton area described as B, folds by Talbot

(1964), and most of the folds described by

Omer & Fleming (1968) as F, folds within

large areas of the Mt. Lofty Ranges. They are

mainly inclined and asymmetric with eastern

bmbs of unticlines longer than western lintbs.

and with axial planc cleavages which dip

steeply to the SE. In many instances, disloca-

tion of the overturned western limbs of -unti-

clines has taken place along faults thar tend to

purullel Lhe axial plane schistosity. All struc-

tural data for this section of coastline are sum-

marized in Fig, 5 which shows the following:

(9) poles to bedding (S,)) indicate a fold usis

estimated to: plunge towards 047° at a low

angle, although mesoscale F, folds plunge

al Variuble angles towards both the NE

and the SW:

(b) intersections of §, with cleavage (8,),

long axes (L,) of phosphatic nodules Cin

the Heatherdale Shale), and the elonga-

tio of boudins resulting from: the defor-

mation of cale-silicate bands within the

overlying Kanmyntoo Croup are parallel

ta the axes of mesoscale F; folds;

phate nodules und ealc-silicate boudins

define a great-circle distribution which

may be the result either of refolding or of

inhomogencous strain;

{di a lineation defined by the elongation of

calcite and mica crystals on $, surtaces

{not heddiny surfaces as reported in

Daily & Milnes 1971u, p. 207) in eal-

eureous and pelitic intervals respectively,

pitches up to 20" more steeply than 1,,,

und is now interpreted as a first-gencra-

tion structure Li’ (not a-sccond-generation

xtruciure as suggested by Daily & Milnes

197ta). The preferred orientution of horn-

blende poikiloblasts and. chlorite porphy-

roblasts. on §, surfuces in cale-siliegte

hourtins. and pelitic tntervals respectively

is approximately parallel to Li’, but its

significunce is not understood.

' This new name is defined herein to inchide all the Lower Cambrian sediments between the bise

of the Mount Ternble Formation and the base ot the Carritkalinga. Head Formation as mapped

in the Sellivk Llill-Normanville area by Abele & MoGowran (1959) and revised by Daily (1963),

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN)

FOLD. PHASE PLANAR ELEMENT LINEAR ELEMENT

: S + surface

Spe peaning

Tihat generatien

elructures

+y S)=Schielmeity Ly 7 Uheation ar

eis ut dott iw

My with Sy as

welal su fface

by = olnerar

1 Plonyation in Sy

Second generation

alruciures

hy S.=—crenulalion

7 cleavage,

Asia! Burtace

ta Fy tots.

Lo bineation gr

Beis af told or

granulation ia,

or Wilh S;

ay ania Surtace™

[i renresents ¢elimated direction and plunge of fold aais,

ah.

a Peo AyHO47 s1meeD®

Pa ms

Miage i" |

*., /

\ i 4. : - f

“\ t d y

e Poles to Se

A Poles to S-

se ee + F Fold gees

2 &, Sleavage/hedding jntersecvons

VY lLoeasleite, cise slangailyds im Sy

Fig. 5. (Above)—Table of structural elements

and corresponding symbols utilised in the

text.

(Below }—Equal area projection of struc-

lural daty for the section between Madi-

gan Inlet and Tunkalilla Beach.

Structural data for the remainder of the type

section and the region east to Middleton are

as follows:

(i) Turkalilla Beach to Rosetta Head

All the macroscale folds mapped and most

of the mesoscale folus observed to the east of

Tunkalilla Beach are interpreted as F, struc-

lures, They cojiltrast with the style of the

regional fold ta the west (mentioned above)

in that the western anticlinal limbs are not over-

turned, The folds are however mainly asvm-

metric with western antichnal limbs stecper

and shorter than the eastern limbs although

towards Rosetta Head the folds tend to be

more upright, symmetrical and apen (Fig. 36),

In yeneral, folds in metasandstones are oper

223

structures Whereas folds in the metasiltstones

and schists. particularly within the Petrel Cove

Formation, are smaller scale structures that

tend to be moderately tight and upright. The

transition [rom one style to another within the

metasandstones cannot be pin-pointed, Our ob-

servations suggest that it is gradual, and it

seems significant that the highly appressed F,

folds are characteristic of the oldest parts of

the stratigraphic sequence, whereas folds in

progressively younger formations are more

open and upright. ‘Vhe validity of this proposi-

tion is strengthened becatise on Dudley Penin-

sula, Kangaroo L.,.and along the Mount Barker

Creek. comparable situations pertain on the

eastern limb of the regional anticline.

The axial plane schistosity in F, folds is

defined by the preferred orientation of micas

which commonly enwrap small quartz-rich

aggregates and, in some localities east of New-

land Head, cordierite porphyroblasts. The

resulting augen define a unique augen-layering

parallel to S, (Figs. 34 & 35; Talbot & Hobbs

b9G8). In the schists est of Newland Head

there is a distinct but often discontinuous linea-

tion due to the elongation of augen on §, sur-

faces (Fig. 53). ‘This lineation is decidedly

different in orientation from that of the inter-

section of S, and 8, surfaces and the axes of

F, folds.

A weak crenulation of S, is apparent in

phyllites near Coolawang Creek and bevomes

more distinct eastwards, This crenulution pro-

vides evidence for the overprinting of first-

generation structures, In some areas there is a

penetrative strain-slip cleavage (Sa) which is

axial plane to mesoscale second-gencration

(F.) folds, Such folds are most cofispicuous

adjacent to pre-F., metamorphic pegmatites

(Fig. 54), They tefold small-scale F, folds

(Figs. 54 & 55) and are responsible for the

local variation in the plunge of F, fold axes

from NE to SW. It should he noted that in the

Rosetta Head region, Talbot & Hobbs (1968,

p. 584) have pointed out “that several sets of

crenulation cleavage are developed lacally”, We

have mapped only one crenulation cleavage

(S,) in that area,

The distinctive “striped” layering (S,)

referred 10 above is best developed just west

of Petrel Cove, Talbot & Hobbs (1968) also

reported ifs occurrence in the Kanmantoo Mine

area in metasediments assigned by Duily &

Milnes, (1972a) to the Tapanappa Formation.

The “striped” liyers are zones of alteration and

consist predominantly of quartz and plagioclase

224

wilh seme muscovite. They are up to 3 tm

wide, anu ure often bordered by thin biotite-

rich zones. I tiddition they may show a median

biotite nu/ or qual'tz-filled fracture (Fig. 56)

Althaugh ihe “striped” layering cuts across S,.

i fellct Sy schistasity. outlined by the preferred

orientation of muscovite and rare biotite, can

be seen within the “striped” layering. Struc-

tural relationships show thar the layering ts

not only post, but clearly pre-Fa (Figs. 43

& 46), Talbot & Hobbs (195, p. 585) sug-

pested thal the “staped” layers are “hon dilata-

tional and represent same form of differentia-

tion process. in situ’. In wew of the presence

of a central fracture within the “striped” layers,

the refraction of Inyenng across bedding, and

Fouthering, we can only conclude that these

structures ure dilatational anid wre due to ten-

sion and subsequent alteration adjacent to the

Fractures,

Alt structural data. collected between Tunka-

lilla Reach and Rosetta Head ate given in Fig.

® a=d. This shaws the following: Poles 10 3S,

show a great-circle spread and indicate a [old

axis estimated to plunge at 25> towards 200°

(Fig. 6a), This is supported by the attitudes of

Ly lineations defined mainly by the intersec-

fiun of S, ad.S, surfaces (Fig. 6b), However,

uxes Of mesoscale Py folds are distributed

about Wo point maxima, indicating plunges

towards the NE and the SW at shallow angles

(Fig. 6c). This suriition in plunge together

with the significant spread of poles to S, (Fig.

fe) may indicate refolding of the first-genera-

ijon ytructures, or may be dug to differential

strain. Ls lineations (the axes of crenulations

jn S,) plot as a diffuse maximum giving an

estinvaled plunge towards 165" at 63° (Fig,

ful =

(ii! The Brawn Hill drea

In the Brown Hill area, large scule NE plung-

ing asymmetric F, folds in Balquhidder Forma-

Gun metisedimenis occupy 4 narrow NE trend-

ing zone. The folds gre upright, and have the

open style typical of F, folds in metasandstones

in the eastern part of the type section. The

axial plume schistosity is defined by the pre-

ferred orientation of micas, A lineation formed

py the intersection ol 8, and S,, surfaces is

parallel io F, fold axes, $, surfaces in pelites

contain a mineral lineation defined by the pre-

ferred orientation of micus. This lineation has

a sleep southerly pitch in $,, and is interpreted

B, DALLY and A. Ro MILNES

usu firsi-veneration seructure (Loy. It is best

seen in the Lincoln Park quarry, south of

Brawn Hill.

The structural elements meastired in this arca

ure plottel in Fig. Ge, Poles to Sy lie along a

greal circle, and imuicule an Fy fold axis esti-

muted to plunge at 35° towards U51°. This is

supported by the attitudes of 1,’ lineations.

Two measuted L,’ lineations plinge steeply

towards the south,

Gil The Middletant A rect

Fust of the Brown Hill area, Fy, folds in

metasediments assigned to the Petrel Cove For-

mation and the Middleton Sandstone have been

overprinted by large- and small-scale Hy folds

that plunge at shallow angles towurds the SE

The relationships between F, und Fy siruc-

lures, both of which exhibit varving deerves. of

development in the area, wre besr examined tn

the Micdkdlelton quarry wbout L4 km NW ol

Middleton.

SE plunging F.. lolds are the deminant siruc-

tures in the Middleton quarry, und are

moderately uppresstd, inclined folds im which

the northern limbs of anticlines are longer thin

the southern limbs, and tend to he overturned

(Fig. 57). The larger folds contain small-scale

refolded Fy folds in pelitic units (Fig, 48),

A prominent set of fractures occurs in 14,

folds in metasandstones and purallels the

weakly developed axial plane schistosily of

these folds (Fig. 57). The intersections of the

fractures {S.,) with the bedding detine wu ridge-

und-furrow lineutian which parallels the F,

fald axis and is referred to here as La (Fig.

59). These fractures have lirvely controlled

albitisition and the ¢mplacement of thin peg-

matites. They have also been planes of past-

alternation movement ulong which either thin

cuatings of fibrous hornblende or hrecciated

zones have developed.

Inspection of the metasediments in the

Middleton area shows that three schistosities

ure present. 4 well expressed axial plane whit

tosity in some mesoscale folds in fine grained

metasandstones can be seen in thin sections

to crenulate a poorly developed older schis-

losity that is approximately parallel {o bedding

(Fig. 60). Moreover, an examination of the

axtal plane schistosity surfaces. shows u con-

spicuous mica-streaking lineation tbat is not

parallel to the fold hinges (Fig. 613. The

presence of two schistosities in these folsis

= Mésosealé Fo totds are Wneommon. but gencrally oceur nenr jhe margins of pre-Fu pegmatite dykes

in jhe Petrel Cove Formation, No wllempl was made to measure their attitudes in such localities,

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN) 225

+ Poles to So

8,= 200° ptunge 25 ® L)= cleavage/bedding

intersection

Vi Le=calc-silicate rod

MN elongation

4 Poles io S,

o Ll

+ F, Fold axes 2

A FoFold axes

A,= 051" plunge 35° 8,= 118° plunge 50°

Poles to Sq

Pol

Poles to Sj * Hes: te Sg

dene

Lif

Fig, 6. Equal area projections of structural data. a-d, Tunkalilla Beach to Rosetta Head; e, Brown

Hill area; f, Middleton quarry.

22 RB. DAILY and A. R. MIT-NES

would normally identify the folds as secund-

generation structures. However, small scale Fy

folds in the Middleton quarry are characterised

by a poorly-developed axial-plane schistosity

(S) that overprints a

developed schistosity parallel to bedding. In

these folds. it is the older schistosity that con-

Wing @ prominent mica-steeaking limeation

whieh as similar in nature and orientation to

lig L,’ lineation recorded in metasediments in

ihe couslal part of the type section and in the

Brown Hill area In the Middleton quarry. Lhis

mica-streyking lineation is readily seen on the

surfaces of F, folds, where it is oriented at a

significant ungle to the intersection bewween

bedding and S, (Fig, 621. In view of these ab-

servations, we presently interpret the meso-

seale folds of uncertain uffinitics. os first-

pencration siructires that formed in metiasedi-

ments containing a pre-teetonic bedding pline

schistosity, and the accompanying prominent

micu-streaking lineation as by‘.

F,, olds were nol observed in the rather poor

exposures outside the Middleton quarry, o i

the small quatty expasures NW of Port Ri hat,

In these foculities, folds also hesitantly inter-

ptered as first-generation structures form the

dominynt sttuctueal clements. They are best

seen i the exposures to the north of the

Middleton quarry. They are inclined, and

plunwe jd steep angles towards the SE. The

uXial plane schistosity is a pronounced mica-

preferred urientalion which again overprints a

pourly preserved presumed pre-tectonic bed-

din-plune schistosity in some specimens, The

imerseation ot bedding with the axial-pline

sclisiusity is parallel to the axes of the folds,

However, a prominent micd-streaking lineation

oa schistusity surfaces pitches up to 20° from

the intersection between bedding, and the axtil-

plane schistosity-

S, Satiaces in phyllites of the Petre! Cove

Formation exposed inthe quarries NW of Port

Elliot and in the cuttings along the Crow's Nes!

road cxhibil a fine-scale crenulation. ‘The creou-

lalion appears to have a similar orientation to

the conspicuous mica-streaking lineation { pre-

sited L,') on $, surluces in metasandstones

in the Middleton urea, but ts interpreted a3 a

secomiu-poueration structure.

Theexposures of Middleton Sandstone along

the coasuine at Middicton are dominated by

F,, Structural clements. A proninent ridge-and-

lurrow linewtion (L.) indices a shallow

easterly-plunging fold. This ayrees with the

moderuicly well-:

orientalion of the fold axis of the only Fold

recorded along the beach.

The geometry of the structural elements for

the Middleton sree are given in Figs, 6f, Tae

und show the following: Poles to S, measured

in the Middleton quarry (Pig. 6F) do nut re-

flect the attitudes of firscgeneration folds, burt

define and F. fold axis estimated to plunge

towards LL&° at SO". This agrees. with the atti-

tudes of measured Fy fold axes and L,, ridye-

and-furrgw tinealions (Mig. 7a), In addition, it

is Consistent with the distribution of poles un

S. fractures in melasandstones.

The distribution of measured mica-streaking

hnewtions in the Middleton quarry indicates an

estimaled plunge towards 122° at 65°, whilst

the attitude of the related schistusity indicates a

stecply-plunging inclined style for folds herein

interpreted as first-generation structures (Fig.

7b).

The structoral elements Sy, and 1... measured

in the exposures at Midulleton Beach define an

F., told axis estimated to plunge at 28" tawards

NYO", and this is supported by the attitude of

one mesoscale F,, fold uxts (Fig. 7c).

In all other parts of the Middleton area,

presumed first-generation structures are domin-

ant, Poles to S, define an B, fold axis csu-

mated to plunge at 60° towards 142° (Tig,

7d). The rather diffuse distribution of S, poles

on the western side of the diagram may reflect

the influence of second-generation folds, ‘The

attitude of the F, fold axis is confirmed by the

distribution of mica-streaking lineations und the

attitudes of poles to the axiul-plane schistosity

(Piz. Je), and approximately coincides. with

the orientation of presumed first-generation

structures recorded in the Middleton quarry.

BL. STRUCTURAL RELATIONSHIPS OF THE

Encoun?tit Bar GRANITES

The contact between the Kanmantoo Group

metuscdiments (Petrel Cove Formation) and

the Encounter Bay Granites is exposed on

Rosetta Head and Wright |, bat is best

examined on Waiglit 1. because of the excellent

exposures there. Our observations of the rela-

tionships at this contact can be summarised is

tollows.

{) The marginal phase of the Encounter Bay

Granites is a coarse-grained meguerystic

granite, Megacrystte granite sheets of

variable thickness and grain. sixe form

apophyses from the main granite mass,

and ure laracly concordant with bedding

in the Petfel Cove Formation metasedi-

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN) 227

B= 18° Plunge 50°

Poles to So

o bg

4 F53Fold axes

¥ Limica streaking

4 Poles to $4

MN MN

B:=O90" plunge 28

B:=142° plunge 60°

» Poles ta So » Poles to Sg

on lg

A FoFoid axes

B,= 142° plunge 60°

¥ Limica streaking

& Poles to S,

o Poles to Sg

Fig. 7. Equal area projections of structural data. a-b, Middleton quarry; ¢, Middleton Beach; d-e,

Middleton area excluding the Middleton quarry and Middleton Beach.

ments TFig. 63). The granite sheets dre

murkedly boudinaged in places,

[h) Petrel Cove Formation metasediment, in

contaer with the megacrystic granite, hoth

on Wright I. and Rosetti Head, are lim-

inated metasiltstones, A paucity af porphy-

roblastic andalusite and cordierite schists

adjucent tn the contact compared with

their abundance at lower straliyraphie

levels Within the formation further from

the granite was noted,

Petre] Cave Formation metusediments anil

@ pafallel schistosity occurs In the borders

and constricted portions of \he boudinnged

megaerysiic granite sheets (Fig. 64). The

same schistosity is variably developed

within the marginal metre of the main

granite mass. Within the affected granite,

the schistosity (Fig. 65) is defined by al-

ternuting laminae of recrystallised biotite

and quartz, which cnwrap latge potash

feldspar and pligioclase megacrysts. Al-

though recrystallised along their margins,

these megucrysts retain their original inter-

nal structures: some have been rotated.

The schisloxe gronile muy be regarded as a

protomylonite using the terminology of

Hiseins (1971). However, we believe that

the schistosity has been imposed during

regional deformation at a moderately high

temperature. The variable development of

the schistosity in the srinite along the

contact. 1ogether with its absence from the

internal parts of the pluton, gre duken ws

eVidence for the high yield strength of

the granite at this time, and suggest thit

the pluton possessed sigh bouy properties

during the regional deformation,

Metisciliimentury-rock xenoliths within the

megacrystic granite awoy [rom the con-

act ure devaid of deformation structures

and, with few exceptions. tectonically tm-

posed miga-preferred orientations. More-

aver. xenoliths containing andalusite or

corilierite porphyroblists have not becn

observed.

(el Structures younger than the S, schistosity

occur wilhin the metascdiments and

wranite sheets on Wright 1, and include

fine scale crenulations in the 5, schistosity.

Broad scale kink-folding of bedding add

thin eranite sheets has alsa been noted,

On the southern side of Wright 1., a cata-

clastic zone crosses the contact and has

deformed the S$, schistosity. Catactastic

(al)

Kk IALLY and A, Re MILNES

TOAtUIES are CONspicuoUS in the granite.

and are strikingly different from textures

in the schistose granite.

C, Summary

The observations anc meastirements of

structural elements indicate two malt phases ot

deformitiun of Kanmantoo Group metascdi-

ments in the type section. With the exception

of parts of the Middleton area, first-generation

structures ate dominant. However, second-gen-

eration structures are moderately well devel-

oped in the Petrel Cove Formation between

Rosetta Head and King Beach, and are domin-

ant in. Middleton Sandstone in the Muldleton

quarry and at Middleton Beach,

There ate several structural observations thut

will only be adequately explained after the

camipletion of a more comprehensive investi-

gation of the structural geology of the Kammun-

too Group than was attempted here, Such ob-

servations include the variable development of

structural elements in the type section, and the

variability in style aod urientation of first

generation folds. Notwithstanding, the data

presented herein provide an adequate basis for

an interpretation of the time of emplacement

of the Encounter Bay Granites in relation to

the structural deformations recorded in the con-

liguous Kanmantoo Group metasedimentary

rocks. The following observations are con-

sidered most pertinent to this discussion;

(a) The prominent schistosity that aceurs with-

in some parts of the megacrystic granite

along its contact with the Kunmuantoo

Group metasediments, and in boudinaged

grantle sheets: wilhin metasediments auja-

cent to the contact, is parallel 10 the S,

tchistoxsity in-the metasediments; and

metasedimentary-rock xenoliths that occur

within the meguerystic granite away from

the contaci. are. with few cxeeptions, de-

void of lectonically imposed mici-

preferred orientations,

Thus the Eneounter Bay Grnites ate con-

sidered to have been emplaced prier to the

main phase of first-generation deformation and

are, in (his sense, pre-tectonic, The texture of

the schistose granite indicules that the meyi-

crystic granite had completely crystallised prior

to the imposition of the $, schislosxity during

the main deformation phase,

Although second-generution structures have

overprinted the 8, schislosity in the metasedi-

ments and in ihe biotite-rich borders of the

granite sheets on Wright 7, their sporadic de-

velopment bas prevented ar) assessinent of their

fh)

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMRBRIAN)

effect nn the granites an a broad scale. On the

other hand, second-geheration structures pro-

vide an important teference point in a discus-

sion of the relative ages of pegmutite and meta-

dolerite dykes. For example, hoth peematites

und metadolerites occur ag transgressive dykes

within the Petrel Cove Formation, and do not

exhibil first-generation structural elements,

However, they have heen folded and houdin-

aged during the second phase of deformation,

Ir fact, second-generation structures, inchiding

mesoscopic folds and an obvious crenulation

cleavage. are commonly hest developed immed-

dutely adjacent to these dykes, On the basis of

these observalions, the pegmatites and meta-

dolerites appear to post-+late the first-generation

folding and pre-date the second. Similar rock-

types idtrudiog melasediments further west

in the type section are probably of the same

age, although this cannot be confirmed because

of the iipparent absence of second-generation

siructures in these areas,

Metamorphism

Published studies on the metamorphic pet-

rology of the type Kanmantoo Group have

centred around the metasediments in the

vicinity of Rosetta Head. From that area

Browhe (1920) first recorded the presence of

indalusile und cordierite . Later, Bowes (1954)

subdivided these metuseciments into three

groups, namely quartz-blotite schists, anudulu-

site and cordierite schists, and albite and chlor-

ite schists. Both Browne and Bowes regarded

the metamorphic assemblages as a consequence

of the emplacement of the Encounter Bay

Granites. On the other hand, Offler & Fleming

(1968, p. 259) recognised “snowball” Internal

fabrics in (he andalusite and cordierite porphy-

roblasts in this area and suggested that “since

the Victor Harbor Granite does not appear to

have been emplaced forcefully. such fabrics

could only have been produced during a defor

tation phase before the intrusion of the gpran-

ites. As shown below cordierite is mainhy pre-

(o warly svn-F, whilst andalusite is late syh- to

post-F, and pre-F,,,

For that part of the type Kanmantoo Group

west of Tunkalilla Beach, Daily & Milnes

(T971u) concluded that the metamorphic arnde

lay between the almandine and slaurolite isa-

studs as defined by Winkler (1970+, and with-

in the andalusile-staurclite zone of OMer &

2349

Fleming (1968). Although our estimate: of the

prade still stuns, we realize that our inter-

pretation of the metamorphic history was over-

simplified. In the present context we have

uttempted to link the various mineryl assem-

blages to readily identifiable structural elements

in the rocks and thus deduce the retative time

relations between crystal growth and deforma-

tron in the fashion of Zwart (19631, Spry

(1963) and Offer & Fleming (1963), How-

ever, this method cannot give a measure of the

time between the various structural and zon-

comitunt metamorphic phases, nor can it allow

one to assess the time tiken for the essential

metamorphic reactions to produce the mineral

ussemblages seen today. Tt is most likely thr

the various recagnisahle metamorphic phases

discussed below are but part of a continuum,

It should be noted thal all the following ob-

servahions and the conclusions drawn from them

pertain only to rocks in the type section of the

Kanmantoo Group as specified by Sprigg &

Campana (1953) and jin our extension of the

type section into the region between Brown

Hill and Middleton Bench, which we regard

48 helonging to the uppermost part of the Kan-

mantoo Ciroup in the castern Mt. Lofty Ranges.

Within the Kanmantoo Group conspicuous

metamorphic mineral assemblages are uncom-

mon, and are confined mainly to thin cale-sili-

cate banifs and lenses and to satne pelitie inter

vals, All nictusediments except the phyllites re-

tain aspects of Iheir original detrital nature

despite the deformation and metymorphism,

The following assemblages of minerals? scem

to be representative of the vurinns rock types

wilhin this region:

(a) metasandstones and metasillstones—

quartz + plagioclase + biotite ++ musco-

vite = calcite + chlorite 7 garnet

scapolite = epidete;

(hd phythtes—

quariz — plagioclase + biotite + muses-

Vile = chlorite + varnct + andalusite +

cordierite;

(¢) carbonaceous and sulphide-rich phyilites—

quartz + plagioclase + muscovite +

pyrrhotite + graphite;

cale-silicates—

quariy | plagioclase + hornblende = gar-

net + chlorite + calcite = biotite + mus-

covite = pyrrhotite “= epidote.

(d)

* Offer & Fleming (196%) have reported fibrolite in many schists within the Mi Lofty Ronges. We

had nal seen thts mineral in our thin seetions until Dr. R, Ofer located am isolated patel in a thro

seciion of metasandstone collected 200 m east of Bollaparadda Beach,

134

AS uv fesult of a petrographic study of the

Kanmantoo Group rocks collected during our

traverses, ihe following scheme of progressive

mctamorphic crystallisation is envisaged:

A. Pre- te Syn-F, Metamorphic Crystallisation

Metamorphic elements attributed to this

phase of crystallisation inglude small quartz-

rich aygtexales, groundmass. biotite and mus-

covite, porphyroblasts of biotite, andalusite and

rare chlorite, and cordierite augen, the latter

commonly altered to a brownish-yellow clay

mineral determined hy electron probe analysis

as kuolinite.

BiotLe porphyroblasts occur with ground.

mass micas throughout the region, but the

quariz-rich aggregates seem to be restricted to

the remon hetween Tunkalitly Reach ard Bn-

counter Ray. Cordicrite is more severely restric-

ted, bein found only in some phvilite hands

in the upper part of the Balquhidder Forma-

tien, and mm the Petrel Cove Furmation neni’

Rosetta Head

Metamorphic clements of pre-F, age ore

uncommon but include many small quartz-tich

ugercgutes containing feldspar, opaques and

micas (Figs, 66 & 67), Their grain size is

always finer than that of the same minerals in

ike groundmass. They form augen which

generally contain a randem internal mica fab-

Tic and arc enwrapped by the well developed

mica schistosity. However, same quurtz-rich

uugen that have been observed with a poorly-

oriented mica fabric may be partly syntectonic.

Some cordicrite augen in the Petrel Cove Fors

mation exhibit a random inclusion fahrie und

represent pre-P, crystallisation.

Metamorphic elements formed during the

first. phase of deformation include the minerals

that define the S, schistesity, namely biotite

and. muscovite. Fer the most part, syn-F, bio-

tite and’ muscovite are fine grained, Medium-

grained biotite and chlorite parphyroblasts of

this age have been noted, 5, is also commonly

marked by u preferred orientation of opaque

mineral laths, for example Fig. 66. Many cor-

dierile wugen which are enwrapped hy $4 show

oriented inclusion fabrics, that are cither planar

and inclined at a significant angle to 8. or are

S shaped (Figs. 67-70). Such fabrics are con-

tinuous with the 8, schistosity in the enclosing

rock. Moreover, as inclusions within the por-

phyroblasts are finer than the same minerals in

the groundmass, we conclude that cordicrite

crystallised and was rotated during, the early

Stages of formation of 3, -

B. DAILY amd A. R. MILNES

Andalusite commonly occurs as S-shaped

poikiloblasts containing S-shaped inclusion-

trails that are continuous with the external S$,

schistosity (Fig. 71)_ Such poikiloblasts are the

result of late syn-S, crystallisation ond rotation,

In some cases the outer margins of poikilo-

blasts cut across this schistosily and must ihere-

fote represent post-S, crystallisation (Fig, 72)

H. Past-Fy Metamorphic Crystallivation

The major porphyroblastic crystallisation

appears to have occurred during the post-F,

and pre-B, static phase when andalusite, gur-

net, hornblende, biotite, chlorite, muscovite.

scupolite and epidote crystallised in rocks of

appropriate lithology. These minerals cut across

the groundmass S$, schistosity, but are de-

formed by the $. crenulation cleavage in rocks

in which this structure is developed, The fol-

lowing conspicuous minerals aid mineral

assemblages are characteristic of this meta-

morphic episode:

ta) calc-silicates—

hornblende “4 plagioclase +

chlorite + epidote,

metasanrstones and metasilistenes —

muscovite + garnet = chlorite + epidote;

= jndalusite = chlorite =

garnet + scapolite + biotite.

In addition, {here are several miner com-

poncots such as tourmaline, some opaque

minerals and sphene which appear to have

crystallised across the groundmass $5 schis-

fosity, and are similarly attributed to this meta-

morphic episode.

Post-5, andalusite occurs both as over-

growths on svn-S, poikiloblasts (Fig. 72), and

as poikiloblasts that have overgrown the

groundmuss §, schistosity and have retained

relicts of this in the form of oriented opaype

laths and quartz grains (Figs, 73 & 74), In

addition, post-S, chlorite (Figs. 75 & 76) and

less commonly muscovite occur in phyllites and

metasiltstones throughout the type section as

Poikiloblasts that have grown across $4. Scapo-

lite occurs as small porphyroblastic clots that

appear to have grown across 5, within meta-

siltstones, 1 kr east of Coolawang Creck-

Porphyroblastic zoned garnets (Fig. 77) may

occur with minor muscovite, chlorite, epidote

and tourmaline in mcetasiltstones and metasand-

slones throughout the lype section, These have

eTown across the S$; schistosity. Such garnets

aré conxpicnous in the heavy mineral sand

suites along the southern coastline.

gatmec

(b)

muscovile =

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN)

Although an interpretation of the textural

relutionships im most rocks éiggest that the

crystallisation of cordierite preceded that of

undulusite, co-exisling post-F, cordierice

poikiloblasts and andalusite euhedra occur in

pelites within 1 m of a metadolerite dyke about

half way between King Beach and Rosetta

Hew. As structural evidence indicates that the

metadolerite intrusions are pust-F, but pre-F.,,

the cordierite-andalusite assemblage is inter-

preted as being the result of a local increase in

temperature along the dyke margins.

Post-F, culc-silicate segregations occur

throughout much of the region and possess a

weakly defined relict 8, schistosity that con-

trasts with the better defined schistosity of the

enclosing mietasedimeots. Hornblende poikilo-

blasts (erroncously identified optically as

actinolite by Duily & Milnes 1971a} occur in

the cale-silicates and, at best, exhibit only a

moderaic depree of preferred orientation

parallel co the relict S, schistosity. Some horn-

blendes. transverse to S, contain undeflected

remnants of that schistosity, especially opaque

faths. Zoned varnets occur in the cale-silicates

ws subhedral poikiloblasts that cut across S,

but these also have inherited the 5, schistosity-

Post-P, metamorphic minerals that occur in

peliles in the eastern part of the type section,

where the S., crenulslion cleavage is best de-

veloped, ure deformed by Sy. The cislocation

of chlorite and undalusite poikiloblasts along

zones commoniy defined by trains of opaguc

minerals grains (Fig. 78), are especially evi-

dent in pelites In the Petrel Cove Formation

in which Sy assumes the characteristics of a

stramn-slip cleavage,

Many pegmiutites within the type section are

composed of minerals that characterise the

post-F, mineral assemblages in the host rocks.

On structural evidence, such pegmatites are

post-F; and pre-Fy and represent the “sweat”

products concentrated in regions of low pres-

sure gtadient (Rivalenti & Sighinolfi 1971)-

Wall-rock alteration has been noted adjacent to

some of these pegmatites.

C. Conditions of Metamorphic Crysiallisaion

A petrographic examination of Kanmantoo

Group metasediments in the type section seems

to indicate a relatively simple sequence of

Metamorphic crystallisation, This sequence be-

gan with the formation of quartz-rich agere-

gates and the crystallisation of cordierite dunng

the pre- to easly syn-F, phase of deformation,

was followed by ihe late syn-P, crystallisation

of andalusite and chlorite and ended with the

231

post-F; crystallisatioi ot andalusite, chlante,

gamel, hornhlende, muscovite and scapulite,

Offler & Fleming (1968) regarded the meta

inorphic mineral assemblages Whtoughout much

of the Mount Lofty Ranges as churacteristic oF

low pressure, intermediate-type metamorphism,

With reference to the aluminosilicate data of

Newton (1966), they suggested that meta-

morphism in the areas of highest grade

occurred at pressures (Pigiai — Pang) between

3 and 4 kb and at temperatures in the vicinity

of 650°C, The metamorphic minerals in the

Kanmantoo Group metasediments in the type

seclion are certainly consistent. with conditions

of low presstire, intermediate-type metamar-

phism, but are representative of lower tem-

peratures und pressures than the assemblages

upen which Offler & Fleming based their esti-

mate.

The crystallisation of pre- to syn-F, cor-

derite and late syn- to post-F, andalusite in

metasediments in the type section suggests that

the conditions of metamorphisin at this time

Were consistent with the andalusite-cordierite-

muscovite subfacies of the amphibolite Facies

(Winkler 1965). Of several possible para-

geneses fnvolving the crystallisation of cor-

dicrite, the reaction—chlorite ++ andalosite +

quartz = cordierite + vapour (Sieferr &

Schreyer 1970) seems to be consistent with the

observed mineral assemblages, Based on the

experimental P-T conditions for this reaction,

and for the aluminosilicate stability as deter-

mined by Holdaway (1971), the crystallisition

of cordierite and andalusite in metasediments

in the type section probably occurred at pres-

sures below about 3 kb and al temperatures

estimyted to be less than 540°C (Milnes un-

pub. Ph.D. thesis) -

Discussions and Conchusious

As a result of our studies on the upper part

of the type Kanmantoo Group, several facts

emerge from which w nurnher of conclnsions

can be drawn additional to those given in Dally

& Milnes (197tay-.

A. Srratigraphile Relationships

In no instance throughout the whole of the

coastal sections have we been unable to ascer-

lain bedding. Transposition as described by

Talbot & Hobbs (1968) is confined to the

vicinity of Petrel Cove. Most outcrops retain

their gross sedimentary features despite the Lec-

tunis and metamorphism, This is readily dis-

cernible from the accompanying fignres,

232

Vhere appears to be conformity between all

the fermations muking up the Kanmantoo

Group as sec out in Table 1. Phe validity ot thy

straligtaphic scheme is enhanced by the oceur-

reace of a virtually identical sequence on Dui-

ley Peninsul, Kanguroo 1, (Daily & Milnes.

I971b, 1972b}. As Our investigations on. this

ishand ore as vet jacomplete there is still room

for an upward continuation of the sequence

beyond the Middleton Sandstone. The latter

constitutes the youngest purl of the Kanmantoo

Group in the Mt. Lofty Ranges, Lt is worth

nog that in the original definition of the

Kanmantoo Grolp, Sprigg & Campana (1953,

p. 14) stated that “the upper boundary of the

Kanmantoo Group remuins undefined”.

B. The Kungarvoian Movements and Karrnan-

too Group Sedimentation

All the original sediments making up whe

Brown Hill and Wattaberr) Sub-groups in ihe

lype section were clastics which ranged in grin

size From clay to pebbles ut least S em in dia-

meter limestones were absent. Indeed. car

bonate shows up only as pebbles in conglomer-

ates or pehbly sandstones. However, its former

presence as iin accessory is probubly indicated

by epidote-rich bunds in the Midelleton Sand-

sions innit ws the thin calc-silicate sesrecations

and hands in all the other stratigraphic units

within hath sub-groups,

Metasandstone is by far the dominant

lithology throughout most of the Kanmuntoo

Group. The sands were essentially immature

all contained vurying amounts of clay and silt

Lmud) as matnx, Quartz and subordinate feld-

spar were the dominant sand-sized particles ind

were derived mainly from the older Precam-

brian Urystulline basement,

The rapidity of deposition may he giuged

mo only ty the immaturity of the sunds but

alsy trom the dominance of pirallel lamination

within the metasandstones. We Interpret this

type of bedding as a consequence of the high

flow regime that prevailed through much of the

depositional history of the group, Intervals with

cross-bedding and especially current-ripple

lamination are common sind represent deposi-

tion at lower flow power as has been estub-

lished by Simons ef al, (1965), Guy er al,

(1966) and Williams (1967). Aflen (1970,

Figs, + & 6), using some of these experimental

data, hus shown the possible alternative

sequences of sedimentary structures that may

form for yarying graity size with decreasing

flaw power at the time of depasiunn,

‘The sands were taid dowat by currents, which

&. DAILY und A. R. MILNES

over long periods of Lime were largely unidirec-

tional, Measured current directions from sedi-

ments infilling low amplitude scour-channels

wihin the Brown Hill Sub-group indigule dis-

(ribuiion of sediment by currents flowing

generally from the NW quadrant. This is simi-

far lo current directions established for the

uoderlying Inman Hill Sub-group, We have

been unable to detect a decrease in pebble size

towsrds the east for conglomerutes in the

Brown Hill Sub-group, though such aw varalion

is discernible in the underlying Inman Jill Sub-

group. For instance, conglomerates in an aver-

turned sequence of metasandstones at Penne-

shaw, Kangaroo T., contain clasts up to 30 cm

in diameter. In correlative conglomerates in the

uppermost parts of the Tapanappa Formution

near “Tunkalilla Beach, the maximum pebble

size is 7 cm. Uhe grealer distance of transport

for these pebhles is jlso reflected in the lower

proportion of carbonate clasts relative to other

clast types,

The persistence of lenticular conglomerates

und pebble bunds into the upper levels of the

Balquhidder Formation. indicates that the neat-

hy tectonic fands, elevated in response to the

Kingarooian Moyements, periodically contri.

buted gravels to the basin (fur discussion on

these movements sec Daily & Milnes 197 1a, p,

20). Evidence, mamly from Kangaroo L and

Yorke Peninsula, indicates that the pebble

suites were derived from the erosion of a strati-

graphic <equence involving crystalline base-

ment and its uncenformable cover of Lower

Cumbrian sediments, mainly carbonales.. Within

the Balquhiikler Formation the buses of the

sands are sharp. No Atte casts, tool murky or

groove casls were located. The tops of sands

tend tn be similarly abrupt.

In contrast to the sandstones of the Brown

Hill Sub-group. the sundstones constituting the

Middleton Sandstone are much cleaner ane in

Utis regard ure similur to those of the Back-

stairs Massage Formation. They are very well

laminated and the »bundant medium-scale

cross-bedded sets indicate current directions

almost invariably from the west, although some

reversed directions are known. Slumping is

common and always down the fore-set direc-

tron. We do net interpret the slumping as a

consequence of the slope of the basinal floor at

the time of deposition, More likely, it has

resulted from the mass movement of the highly

unstable woter-laden (thixotropic) fore-ets,

perhaps due to current drag, The Middleton

Sandstone on Dudley Peninsula, Kangaroo ,,

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (GCAMBRIAN}

also conustenily shows fore-sets and slumps

thrected cowards the eust,

Load custs on the bases of fpetasandstones

ure common, Occasionally, where soft sediment

formation was more intense. pseudo-nodules

(Macyr & Antun 1950) were formed aid in

extreme cases isolation from the overlying

parent sand was effected, thus permitting the

balled-up sund to sink into the underlying

muds, Exampics of all these structures can be

secn in the Rosella Head area and were figured

by ‘Talbot & Hobbs (1969),

The Kanmantoo Group pelites above the

Tapanappa Formation frequently show aod

sedimentary structures, mainly iamination or

rippled features. The latter range trom starved

ripples, indicating insufficient silt tu fine sand

in the transported fraction ta form a continuous

bed. to sets of climbing ripples. “where sedi-

ment deposition occurs simultaneously with

continuing irinsport in suspension and as bed-

Joad” {Allen 1970, p. f) in the lower flow

regime. The latter structures are indicative of

very high rates Of deposition.

Convolute lamination is not common bul

where it occurs it can efter be traced along

strike for the full length of oulcrup, thus indi-

cating the widespread naturc of the events

which led to its formation,

According to Sprigg & Campana (1953,

Pp. 12) the dominant facies of the Kanmyntoo

Group “are comparable with the Alpine

Flysch"”. Dally (1956, p. 139) stared “It is

believed that shoreline conglomerates, sana-

stones and shales as see in the Kangaroo

Island Group grade seawards into the ‘Aysch-

like Kanmantag sediments which were

deposited in areas of rapid subsidence’. There

is mo doubt that the characteristic alternation

of Metasandstones and pelites as seen in the

Rulquhidder Formation is: ‘“flysch-like’, How-

ever, in no respects can we regard this as o

turbigite facies. For instance, nowhere have we

seen the five-fold division of internal sedimen-

lary slructures which characterise the ‘cam-

plete” turbisile of Bouma (1962). Ta fact, pro-

longed search has fuiled to find the truly graded

and structureless bisal interval which features

so prominently in Bouma'’s “turbidite facies.

model". The tyct that somie grading may occur

within the well-luminwted and ripple-bedded in-

tervals is no criterion of deposition by Lur-

bidity currents because comparable grading

oceurs in sequences deposited in a number of

enviranments, marine and non-marine. In his

critical review of the turbidite problem Vin

235

der Lingen (1969, p. 10) also used the term

“Mysch-like” to cover “alternating, sequences

reuching thicknesses of geosvneclinal magnituule,

bul fackiny typical “turbidite characteristics’ ”.

In our Opinion it is wrong to cquate “fiysch-

like™ sequences with turbillites, be they either

proximal or distal (Wiulker 1967, Table IL, p.

32), or Nuxoturbidites, (Dzulinski er af, 1959).

What must be proved of course is that the

sequences concerned are the products of tur-

bidity currents before they cah be called dur-

bidites. In addition, the terms flyweh and

furbidites conjure up in many people's iminds

the notion of deep water environments, Already

there are many instances Where such iclews are

incompatible with the evidence. for cxample

the discovery of the footprints of birds in some

meas of flysch (Mangin 1962).

The interpretation af the depositional envir-

onment of a sedimentury sequence may be de-

duced only after critical cxuminalion of all the

available cvidence, Rven then no finality need

be reached, In the present context we visualise

the following:

(a) Because of the great thickness of Kanman-

too Gtoup metasediments. subsidence

must have been extremely rupid, Basin

development was probably controlled by:

faulting to account for this.

‘The nature of must of the racks shows thal

sedimentation was rapid. Possibly ueposi-

Lion kept pace with subsidence. There is

no evidence of lemporary emergence, such

as mud-cracks. However, these would he

hard to-Jocate in this metamorphic terrain.

amplitude scour-channels are common in

the thicker sand intervals. The associated

low angle cross-hedued sets (generally less

than | m thick) are typical of deposition

in an aqueous environment. A marine en-

vironment is suggested by the prevalence

of the higturbated tops of some of the

sandicr bands. Severe restriction giving

rise to unfavourable environmental condl-

tions could be invoked to explain the pre-

sumed absence of a benthoni¢ shelly fauna

in the sands. However, such 4 restriction

may be more apparent than real, for in

view of the rapid rate of deposition, the

basinal waters would have contained abim-

dant fines in suspension which may have

heen deleterious to the presence of a Cam-

brian shelly fauna. Assuming a marine en-

vironment, the lack of. reworking of the

sediments indicates that either subsidence

fb)

wus rapid enough to prevent reworking Ur

that sedimentation look place at a depth

below effective wave base. This could have

heen quite shallow (McCave 1971}.

The high incidence of medium scale cross-

bedding and the greater maturity of the

sands of the Middleton Sandstone scem

lo indicate that it was deposited in a

shallower environment than the Balqu-

hidder Formation, It is almost certainly a

shallow water deposit.

In the absence of autochthonous foxsil

assemblages it is impossible to give any objec.

live depth indicators purely on the basis of the

known sedimentary structures. All we can sug

gest here is that the Middfeton Sandstone is a

shallow water deposit, which because of rapid

subsidence escaped reworking, Rocks of the

Balquhidder Formation were — probably

deposited in somewhat deeper water but there

is mo yuarantee of this, We certainly do not

envisage ji deep water origin for it, because un-

metamorphosed sediments of similar facies and

ef shallow Water origin occur on the northern

coast of Kangaroo J, Possibly the deepest water

is indicated by the finely laminated blue-black

carbonaceous and sulphide-rich phyllites indi-

caling stagnant bottom conditions, However,

tven here avery shallow environinent of de-

position Is possible. All that is needed to pro-

dulce sediments of this type is a Call off in the

deposilion of coarser ¢clastics, a restriction of

circulation, and a supply of abundant organic

niatter to produce the carbon and sulphides

under strongly anoxidising conditions.

C. Relativuship of Metamorphism und Strtec-

jure to the Emplecemeth of the Encounter

Bay Granites

Our observations suggest that the Encourter

Bay Granites in the Encounter Bay ares were

emplaced prior to the main phase of first

generation deformation, Moreover, metamor-

phism in this area began with the pre- to eany

syn-F, crystallisation of cordierite and quartz-

rich pgeregates in metasediments of approp-

rule composition, continued with the late syn-

F, etystallisation of andalusite and chlorite,

and ended in the post-P, structurally static

phase during which the crystallisation of an-

dalusite, chlorite, garnet, muscovite, hornblende

und scapolite occurred in metasediments of

uppropriate composition,

Cordierite is restricted to some pelites in

the upper part of the Balquhidder Formation

and in the Pewel Cove Formation along the

Coustal section between Encuunier Bay and

B, DAILY und A. R, MILNES

Pursons Beach and its crystallisation records

the highest grade of metamorphism in the

revion, It occurs as altered augen in phyllite

bunds that crop out in the headland at the

easiemn eng of Parsons Beuch; it has not been

recoghised in racks to the west of this locality.

nor in rocks in the Brown Hill to Middleton

arex, Andalusite o¢curs mainly in some pelites

in the upper part of the Balguhidder Formation

and in the Petrel Cave Formation slong the

coastline east of Newland Head in association

with cordierite, However, ture altered post-F,

poikiloblasts that occur further west along the

cogstline, for example in Tapanappa Forma-

tion metasediments near the western end of

Tunkalilla Beach and at Tunk Head. are con-

sidered to have been composed of andalusite,

Their occurrence 1 consistent with the presence

ot andalusite poikiloblasts in Tapanappa For-

mation metasediments that crop out along [the

northern coast of Dudley Peninsula, just cast

of Penneshaw (Daily & Milnes, unpublished

observations). Minerals sich ag homblende

und garnet, which are characteristic of cale-

silicate lithologies, oceur throughout the type

section, Scapolite however, is confined to cer-

tain pelites that occur 1 km east of Coolawang

Creck.

We have mapped a magnificent development

of syn- to post-F, metamorphic minerals such

as andalusite. hornblende, scapolite and garnet

in Adelaide Supergroup metascdiments which

occur within a thrusted fault block along the

north coast.of Dudley Peninsula, approaintuicly

12 km from the Encounter Bay Granites at

Cape Willoughby (Daily & Milnes 1971b,

1972b). However, there is a conspicuous

paucjly of these minerals itt Kanmantoo Group

metasediments closer to the granites. Thus,

Kanmantoo Group mefasediments in this area

appear, on the whole, to he ef such composi-

tion (for example deficient in alumina and

lime) that they fail to contain metamorphic

assemblages thal are indicators of metamorphic

grade.

The entire type section of the Kanmantoo

Group, as well as the section on Dudley Pen-

insula, occurs within the regional andalusite-

staurolite zune of meiamerphism according to

Offer & Fleming (1968). The presence of

plagioclase of oliguclase-andesine composition

in the metascdiments we have examined is con-

sistent with this grade uf metamorphism. Thus.

the paucity of andalusite in all but parts of the

Balquhidder Formation and Petrel Cove For-

mation west of Petrel Cove is best interpreted

uppropriate hulk composition. The restricted

occurrence also of cordierite mav be due Lo the

limited presence of metasediments of auitable

composition. However, the canspicuuus devel-

opment of large post-F, cordierite porphyro-

biasis near a post-F, metadolerite dyke intrid-

ing metasediments. on the const about half-way

between Petrel Cove and King Point suggests

that varied proximity to a heat source. such as

the Enoounter Bay Granites, may also have in-

fluenced ita development. The absence of cor-

dierite and andalusite and other porphyrahlas-

tic minerals in Balquhidder Formation and

Petre? Cove Formation metasediments in the

Brown Hill to Middleton area. compared with

their abundance in metasediments In the same

stratigraphic position along the coastline west

of Encounter Bay, is patticulariy difficult to

nceount for. It may be the resule either of

inappropriate bulk compositions af metasedi-

ments in the Brown Hill to Middleton area,

pethaps due to facies changes along strike From

the coastal section, or the effect of conditions

af significantly lower metamorphic grade. In

view of the occurrence of plagioclase of olizo-

clase-andesine composition in the melascdt-

ments in the Brown Hill to Middleton area, the

former sugvestion is favoured,

Thus. the relationships hetween structural de-

formation, metamorphism and the emplace-

ment of the Encounter Ray Granites in the En-

counter Bay area, as deduced from field aid

pelrographic evidence. can be envisaged as

Follows:

(a) Regional folding, was initiated, probably

with the development of broad-scale Folds

and the development of an incipient S,

schistosity,

(b) The Encounter Bay Granites were em-

placed, and simultancously incorporated

abundant metascdiment xenoliths, the

majority of which do not display an im-

posed mica-schistosity, Cordierite and

quartz-rich augen crystallised in metasedi-

ments. of appropriate composition adjacent

to the granites, in response to locally ele-

vated temperatures,

event, deformed the marginal granite

phases which had already completely

erystallised, and brought to completion the

development of the penetrative $, fabric

in the Kanmantoo Group metasediments.

Andalusite oad chlorite porphyroblasts

345

erystallised in these metascdiments on a

regional scale as a result of suitable P-T

conditions.

Saniftcant porphyroblaslic yrowth of

metamorphic minerals. occurred during

the post-F; static phase, Post-S, snddalu-

site crystallised us Overgrowths on syn-S;

porphyroblasts, amd us poikiloblasts ad-

jacent to the post-S, striped layering (S.).

Pegmative and ametudolerite adykes were

emplaced.

fe) A second phuse of folding (F.,) deformed

pre-existing structures, including 5S, and

the post-S, “striped” layering, and was

responsible for the development of a cren-

ulation cleavage and a strain-slip cleavage

S.. The main development pf Fu struc-

tures occurs in the eastern part of the type

section, Evidence for metamorphic

crystallisation during or post-dating the

second phase of deformation has not been

observed. However, albitisation and the

crystallisation of fibrous hornblende has

occurred along the §, fracture cleavage,

This 15 believed to be associated with the

widespread fate stage glbitisation (Dasch

er al. 1971) affecting the Encounter Bay

Granites. As well, we have observed tour-

maline filled fractures with orientation

similat to thal of S.,

td)

Acknowledgements

The expenses relating to this work were de-

frayed hy a Grant made to the University of

Adelaide by Beach Petroleum N11 We wish

to thank Mr. R. C, Sprigg for his continuing in-

terest in the project and for arranging the

Beach Petroleum Grant.

We wish to thank Dr. R. 1, Oliver for

his criticigm of the manuseript und for his ¢um-

ments on the metamorphic textures; alsa Dr.

M. A. Etheridge, Dr. A. W. Kiceman, Dr.

P. DB, Fleming, Dr, KR. Offler and Mr. R. G.

Wiltshire for discussions in the field and cam-

ments on an early draft of the structural and

metamorphic sections of the paper.

Tn addition we wish to thank the Drafting

Section, C.S.1.R.0. Division of Soils. for the

preparation of the coloured maps und Profes-

sor J. L. Talbot for the use of his large thin

sections of Petrel Cove Formution metssedi-

ments.

736

B. DAILY and A. R. MILNES

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"Geological Txcursions Wandbuok", 49-54.

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Day, B, & Fonsrus, B..G. (1969).—Notes on

the Proterozoic and Cambrian, southern and

ceniral Flinders Ranges, South Australia, 71

B. Daily (Ed), “Geofogleal Excursions Hand-

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Dawy. B.. & Mirwes, A. R. (1971h)—Discoverv

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on Dudley Peninsula. Kanaaroe Island, Sonth

Australin, Search 2, 431-433.

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of the stratigraphic nomenclature of the Cam-

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geal. Soe. Aust. 1902), 197-202.

Day, RB, & Miners, A. R. (1972h) —Sienificamce

of basal Cambrian metasediments of andalu-

site grade. Dudley Peninsula, Kangaroo

Idand. South Australia. Feareh 3, 89-91.

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166.

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GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN) 237

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Fig.

Fig,

Fig. <

B. DAILY and A. R. MILNES

Well laminated metasiltstoncs within the Tunkalilla Formation, south sidé of Tunkalillu

Creek, Scale in mm (total length 7.5 cm).

. Worm casts etched ott by sand blasting of metasandstones, Bollaparudda Beach.

Well laminated metasandstones occupying a cut-and-fill channel in Balquhidder Kornvation,.

eastern side of Tunk Head. Hammer Iength 28 cm,

Tectonically deformed load casts and associvted flame structures, on the base of a meta-

sandstone, about 0.2 km east of Tunk Head.

Climbing ripple-trains developed in metasandstones jiterbedded with mtetasiltstones, Same

locality us for Fig. 12.

An erosional channel cut into well laminated metasandstones, sume locality as for Figs,

9 .& 10. Channel was filled with shale chips and sands. The hammer is lying against the

bioturbated metasandstones shown in Figs, 9 & 10.

Cale-silicate rods developed in metasandstones and plunging parallel to the fold axis; same

locality as for Figs. 12 & 13.

Thin planar- and irregular-shaped segregations of calc-silicates developed roughly parallel

to the hedding in meétasundstones; same locality as for Fig. 15.

Well bedded and cleaved metasandstanes in the trough of the Tunk Head syncline about

0.6 km west of Tunk Head. Note the well developed sigmoidal cleavage (outlined), ‘The

eavernotis weathering of the rocks is a common feature along the coast of Fleurieu Penin-

sula and on Kangaroo I.

Thick hands of well-banded metasandstones interbedded with thin laminated phyllites,

trough of ‘Funk Head syncline. Note the cross-cutting pegmatiti¢ veins fo the tight of the

figure, 1.8 m tall.

View of top surface of a coarse-grained metasandstooe bed showing smeared out sedimen-

tary structures, Lineation (hammer handle parallels it) is due to a cleavage/bedding inter-

section; same bedding surface as that shown in the bottom left corner of Fig. 18. Sedimen-

lary structures within the central party of the bed are relativcly undistorted by the

cleavage. Only in the uppermost few centimetres of the bed is the cleavage sharply refracted

thus producing marked distortion or iecionic smearing of the sedimentary structures.

Beds: of metasandstones alternating with thinner intervals of less resistant phyllites and

metusilistones; centre of Tunk Head syncline.

Tectonicully deformed cutrent-hedded (rippled) and laminuted metasiltstones interbedded

with phyllites about 30 m west of Tunk Head. Note the abundance of thin ptygmatic pee-

matilic veins,

Sulphide segregstions ane veinlets within a 2 im thick blue-black phyllite/metasundstone

interval, narrow pitch immediately west of Tunk Head.

Fallen block of Balquhidder Formation metasandstone displaying # thin bund of small-

ae conglomerate about 0:4 km east of Bollaparudda Beach. Hammer head lying in plane

of bedding.

Well-bedded coarse-grained metasandstones within the Balquhidder Formation. Note small

granules and pebbles recurring up through the sequence. Lecality abont 0.5 km east of

Bollaparudda Beach. Width of hammer head 17 cm.

Bright orange-red coloured zones of feldspathization developed along closely-spaced frac-

tures within metasandstone beds, 1.1 km eesti of Rullaparuddy Beach. Note paucity of

tensional fractures within the phyllite interbed compared with their greater abundance in

the overlying and underlying metasandstones, However, feldspathised zones do occur along

some of the frachires. cutting the phyllites. Feldspathized zones also occur to the west of

Mollaparudda Beach.

Fig. 3

Fig. 2

Fig.

Fig. 3

Fiz.

Fig-

Fig

Fig.

Pig.

Pig,

Fig.

34.

Lint

3h.

38.

2. 41,

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN| 239

Pegmatites infilling tensional fractures in metasandstones of the Balquhidder Formation 0.7

km east of Coolawang Creek. Note the warping and feathering of the fracture infills.

WellJuminated metasiltstones overlain by current-bedded sets of ripple trains 1.2 km east of

Coolawang Creek, Hummer handle 15 cm Jong,

A_ prominent rib-and-lurrow lineation on the sole of a thick metasandstone bed 0.7 km west

of Parsons Beach. Boat for scale.

Conyolute lamination in metasiltstones west side of Parsons Beach. Coin 2.3 em in dta-

meter,

Small channel cut into a pebbly metasandstone and filled with cross-bedded and laminated

metasandstones, Adjacent to beach on western side of Newland Head.

Fluggy outerops of metasandstones with thin phyllite partings on the western side of New-

land Head. A more massive band of meélasandstone is visible on top of the exposed

sequence.

View looking SW along strike towards Newland Head. Sequence cansists of steeply-dip-

ping metasandstones and interbedded thin phyllites. Included also is a blue-black curbonu-

ceous and sulphide-rich phyllite,

View looking towards Rosetta Head showing the high cliffline cut in the Balquhidder For-

mation, Note the lower cliffline cut in Petrel Cove Formution between King Point (extreme

right) and Rosetta Head.

Pen (14 cm long) is parallel to bedding im metasiltstone bands interbedded in knotted

potphyroblastic schists just below top of Balquhidder Formation, about 0.6 km west of

King Point. Note the pale coloured strain shadows around the aagen aligned in the cleavage

which dips away to the left.

Relationships of various layerings in porphyroblastic andalusite schists occurring near the

base of the Petrel Cove Formation, (Sq} is bedding, (S;) is an augen layering in the

cleavage, (S,) [referred to as (3.) in text) is a pale coloured “striped” layering. Note also

the “pinch-and-swell” quartz-feldspursmicu pegmatilic layers developed parallel ta the

“striped” layering and along which dislocation has occurred. Pen for scale.

A small synclinal fold in andalusite schists plunging towards 210° at 25°. The bedding,

well expressed by the folded darker layers, is also parily expressed by some andalusite-rich

layers, Some steeply dipping fine "striped" layers can be seen cutting the bedding in the left

of the photo. Tip of pen for scale.

Extremely well-laminated metasiltstones in the lower part of the Petrel Cove Formation

about 0.2 km west of King Point.

Current-bedded ripples and other sedimentary structures in well-bedded metasilistones,

Petre! Cove Formation, King Point.

Deformed load casts, their attendant flame strictures, and ripple-trains in metasandstanes

in the Petrel Cove Formation, 0.75 km SW of Rosetta Head wharf. Note thin “striped”

layers: culling the deformed sedimentary structures. Two pale coloured ribs of coarser sand

are elongated towards 210° in the direction of the Fy fold axis, The “striped” laycring is

post Fy as at cuts deformed sedimentary structures. Pen is 14 cm long.

Deformed load. casis 10 m SW of Fig. 39. Kedding dips shallowly to right. Note that the

bedding has been slightly offset by shearing parallel to the cleavage. Noie also the broad

stripe, tight of the coin (diameter 2.3 cm), dips ala slightly lower angle than the cleavage.

The stripe has a thin central dark biotite layer margined by broad pale coloured stripes in

itrn margined by selvages of biotite.

View looking SW at outcrop of shallowly-dipping, well-bedded, fine-grained metasand-

stone interbedded with softer and darker coloured andalusite schists, 0.75 km SW of Rosetty

Head wharf. All beds are cut by a white “striped” Jayering.

240

Fig.

Fig,

Fig.

Fig,

hig.

Fig.

Fig,

ig.

Fig.

44,

45.

ig. 46.

47,

48.

49.

54.

56.

57,

58.

B. DAILY and A. R. MILNES

Note refraction of discontinuous white “striped” layering in schists. steeper in metasand-

stones. Same locality as Hig, 41.

Refracted “striped” Jayering (partly discontinuous) sloping to left and crenulation cleavage

(almost yertical) in andalusite schist, Same outcrop as for Figs. 41 & 42. Nate that the

“striped” layers are slightly folded in some of the andalusite schist layers. The crenulauon

cloavuge (Ss) is axial plane to these folds. No obvious folds occur in the overlying fine-

grained metasandstone which dips to left at a shallower angle than the “striped” layering,

Same outcrop as in Fig. 41. Note the refraction of the “striped” Isyering as it crosses the

andalusite-deficient bands. There they are thickened,

Feathering of “striped” layers in metasandstones of Petrel Cove Formation just west of Petre!

Cove.

“Striped Juyering markedly refracted in passing from metasandstones into interbedded

andalusite schists, Bedding dips steeply to right and occurs on the limb of a fold plunging

towards 205° at 25°. Note that there is a crenulation cleavage axial-plane {0 small-scale

Fs folds confined to the “striped” layering within the andalusite schists, Locality on western

side of Petrel Cove.

Andalusites preferentially developed along some of the “striped” Jayers west of Petre! Cove..

Lens cap 7 cm in diameter.

View from 1.3 km SW of Brown Hill Jooking towards Rosetta [Tead. Note metasandstones

of Balquhidder Formation in foreground sloping down towards lower ground on the ex-

treme left which is underlain by phyllites of the Petrel Cove Formation, ‘This is com-

Parable with the geomorphology to the tight of Rosetta Head just below horizon.

Cross-bedded and welltaminated metasandstones of the Middleton Sandstone near western

extremity of outcrop, Middleton Beach. Scale 11 cm long.

Pale coloured epidote-rich bands in well-bedded fine-grained Middleton Sandstone near wes-

térn extremity of outcrop, Middjeton Beach.

Epidote-rich segregations or nodules occurring parallel to bedding in the fine-grained

Middleton Sandstone, near western extrentity of oulcrop, Middleton Beach.

Pale coloured epidote-rich layers outlining uw markedly croxs-bedded melasandstone unit

(300 om thick) i the Middleton Sandstanc, Middleton qnarry, Sequence is part of the

steeper limb of the Fe fold illustrated in Fig. 57.

View of S, surface in Petrel Cove Formation andalusite-cordierite schist. showing the inier-

section between S; and bedding {I4) and a lineation (T.) defined by the elongation of

andalusite and cordiernte auyen. Length of (Ly) arrow 14 cm.

Fy fold in bedding and in a thin metamorphic pegmatite, Petrel Cove Formation, along

coast between Petrel Cove and King Beach. Note refolded F; folds. Coin 2.1 cm in dia-

meter.

Small-scale Fy folds in bedding in Petrel Cove Formation metasiltstane refolded by Fo fold.

Schistosily, oriented approximately EW in photograph, is Ss. Same locality as Fig, 54. Coin

2.1 em im diameter,

“Striped” layering in laminated metasiltstone in Petre! Cove Fortnation metasilistone, same

locality as in Fig. 41. Note median biotite- and/or quartz-filled fractures, and biotite-rich

margins of stripes. Coin 2.3 cm in diameter.

Lurgé-scale. SE plunging Fo fold in Middleton Sandstone, Middleton quarry. Light coloured

layers parallel to bedding are cpidote-tich, Promincnl fracture cleavage axial plane to fold

has controlled albitisation (light coloured cross-cutting zones). Figure (arrowed) 1.3 m tall.

Tight small-scale F, fold in Jaminated metasandstones on limb of large-scale Fa fold in

Middleton quarry. Scale on right 7,5 ¢m. long.

Fig.

Fig,

Fig.

Fig

Fig.

Fiz.

Pig.

Fig

Fig.

hig.

60.

al.

f6,

47.

a8,

69,

TI.

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN) 24|

Ridge-and-furrow lineation (Lo) defined by the intersection of bedding and fracture cleav-

ge axial plane to Fy folds, Middleton quarry, Scale provided by 5 cm wide compass.

A large thin-section of mesoscale folds: in which w well-developed flaring axial-plane schis-

tosity (S-fold) overprints a pooily developed schisiosity (S) parallel to bedding; Middleton

quarry, Scale cm graph puper.

A specimen of mesoscale folds in bedding from which the section in Fig, 60 was cul, Nole

fald hinges (1-fold). and conspicuous mica-stréaking lineation (I.) developed on. schistosity

axial plane to folds (S-fold); Middleton quarry. Bar scale represents 4 cm.

Small-scale F., fold showing ridge-and-furrow fineation (Le), which is defined by the inter-

section between bedding and the fractufe cleavage axial plane to the fold, Note the mica-

streaking lineation (I.) that occurs on the moderately well-developed $) schistosity

approsimately parallel to bedding; Middleton quatry. Bar scale represents J cm.

Thin concordant granite sheet intruding, laminated metasiltstones of the Petrel Cove For-

mation, Wright fT. Pen 14 ¢m long.

Boudinaged concordant granite shect in Petrel Cove Formation metasiltstones, Wright I.

Note well-developed schistosity in margins and constricted portions of sheet. While spots on

rock surfaces are small marine gastropods, Hammer length 28 cm.

Surface of slab of schistose megucrystic granite. Schistosity, defined by alternating biotite

and guariz-rich laminue. enwraps feldspar megacrysts (light cotoured megacrysts ate plagio-

clase, darker coloured megacrysts are pofash feldspar). Quuriz megacrysts did not survive

the deformation. Specimen collected from main granite mass on NE side of Wright J. within

I m of contact with Petrel Coye Formation metasilistone. Scale in mm.

Pre-S; quartz-rich augen enwrapped by Sy schistosity in thin section of Balquhidder For-

mation porphyroblustic schist SC97", 200 m beyond eastern end of Waitpinga Beach. Note

the preferred orientation of abundant opaque laths in .S;. Transmitted plane polarised light.

Bar scale represents 0.10 mm.

Pre-S; cordierite augen, now altered to kaolinite, enwrapped by gromndmass §) schistosity.

Thin section of Petrel Cove Formation porphyroblastic schist TI30A. Transmitted plane

polarised light. Bar scale represents (0.50 mm.

Field in Fig. 67. Crossed polars. Note fine-grained size of quartz inclusions within altered

cordicrite augen compared with grain size of quartz in groundmass. Bar scale represents

0,50 min.

Syn-S; cordierite poikiloblasts, now altered to kaolinite. Thin section of Petrel Cove Forma-

tion cordicyite schist SC106A. The poikiloblasts exhibit an oriented internal fabric which is

continuous with the external S; mica schistosity, and have been rotated relative to it. Note

post-S; muscovite Juth (M). Transmitted plane polarised light. Bar scale represents 0.50

myitl.

Field in Fig. 69. Crossed polars. Note fine grain size of quartz inclusions in altered cor-

dierite augen compared with grain size of quartz in groundmass, This suggests that cor-

dierite crystallised during early syn-S; phase. Absence of curved internal fabric suggests

cordierite porphyroblasts. were rotated bodily with respect to external 8; schistosity after

crystallisation was completed. Note post-8,; muscovite lath (M). Bar scale represents 0.50

mm,

Syn-S;, S-shaped andalusite poikiloblast (A), with S-shaped internal fabric. Internal fabric

continuons with external groundmass. $1 schislosity. Note post-Si overgrowth on beltam

right of poikiloblast just lefp of post-S; chlorite lath (c). Thin section of Petrel Cove For-

ebnath andalusiie-cor dinrite schist T108. Fratismitied plane polurised light. Bar scale repre-

sents 0.50 mm.

= Numbers prefixed by SC refer to rock sample numbers collected by us Numbers prefixed hy 'T

Tefer to rocks collected by Professor J. L: Talbut.

242

Fig.

77.

78.

B. DAILY and A. R. MILNES

Post-S; andalusite (A) as overgrowths on syn-S; andalusite poikiloblast, Groundmass Sj

schistosity is defined both by micas and by opaque mineral laths. Note sharp contacts be-

tween andalusite “fingers” and groundmass micas. Thin section of Petrel Cove Formation

andalusite schist SC102. Transmitted plane polarised light. Bar scale represents 0,10 mm.

Post-Si andalusite poikiloblast (A) which has crystallised around altered cordierite atugen

(C). Thin section of Petrel Cove Formation andalusite-cordierite schist T135A. Transmitted

plane polarised light. Bar scale represents 0.50 mm.

Field in Fig. 73. Crossed polars,

Post-S; chlorite poikiloblasts (c) which have crystallised across 5; and inherited the S;

fabric, indicated by elongate quartz and opaque mineral inclusions. Thin section of Tapa-

nappa Formation porphyroblastic phyllite SCS50, from ancient cliffline, western end of

Tunkalilla Beach. Transmitted plane polarised light, Bar scale represents 0.10 mm.

Post-S; chlorite poikiloblasts (c) which have crystallised across S, and inherited the S;

fabric, indicated by opaque mineral] laths. Thin section of Petrel Cove Formation andalusite

schist SC102. Transmitted plane polarised light. Bar scale represents 0.50) mm.

Post-S; euhedral garnet (g) and chlorite (c) porphyroblasts adjacent to pre-S; quartz-rich

augen (Q) in thin section of Tunkalilla Formation porphyroblastic phyllite SC58A, eastern

side of Tunkalilla Creek. Transmitted plane polarised light. Bar scale represents 0.10 mm.

Thin section of Petrel Cove Formation andalusite schist SC103 showing the development of

S» strain-slip zones, outlined by opaques. The strain-slip zones cut across post-S; chlorite

porphyroblasts {c). Note andalusite porphyroblast (A). Transmitted plane polarised light.

Bar scale represents 0.50 mm.

244 B. DAILY and A. R. MILNES

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN) 245

246 B., DAILY and A. R. MILNES

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN) 247

248 B, DAILY and A. R. MILNES

GEOLOGY OF TYPE SECTION, KANMANTOO GROUP (CAMBRIAN) 249

B. DAILY and A. R. MILNES

= a

~ ar

eae

GEOLOGY

‘t

-—-

ps 2 AN ae

ess Sees

Lon es ae

VOL. 97, PART 4 30 NOVEMBER, 1973

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Womersley, H. B. S. Further Studies on Australian Kallymeniaceae (Rhodophyta) 253

Mawson, Patricia M. Amidostomatinae (Nematoda: Trichostrongyloidea) from

Australian Marsupials and Monotremes - - - - ae 257

Mills, K. J. The Structural Geology of the Warren National Park and the

Western Portion of the Mount Crawford State Forest, South

Australia - - - - - = “ se = =” DM:

OBITUARY: THEODORE GEORGE BENTLEY OSBORN, D.Sc., M.A., F.L.S. 317

Annual Report of Council, 1972-73 - - - - - “ z = . 391

Award of the Sir Joseph Verco Medal - - - - - - - = 322

Balance Sheet - - - - - - 2 a = - S aye are)

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

FURTHER STUDIES ON AUSTRALIAN KALLYMENIACEAE

(RHODOPHYTA)

BY H. B. S. WOMERSLEY*

Summary

WOMERSLEY, H. B. S. (1973). -Further studies on Australian Kallymeniaceae (Rhodophyta).

Trans. R. Soc. S. Aust. 97(4), 253-256, 30 November, 1973.

Further collections since the monograph of Womersley & Norris (1971) extend the range of

Kallymenia cribrogloea into N.S.W., clarify the structure and relationships of K. rosea and

K. polycoelioides, and show that Cirrulicarpus australis and Meredithia nana are one species now

known as Cirrulicarpus nana (J.Ag.) comb. nov. Callophyllis coccinea is now referred to as

C. rangiferinus (Turner) comb. nov.

FURTHER STUDIES ON AUSTRALIAN KALLYMENIACEAE (RHODOPHYTA)

by H. B. S. WomMersLEey*

Summary

Womersiey, H. B, S. (1973).—Further studies on Australian Kallymeniaceae (Rhodophyta).

Trans. Ry Soc. S, Aust. 97(4), 253-256, 30 November, 1973.

Further collections since the monograph of Womersley & Norris (1971) extend the range

af Kallymenia eribrogleea into N.S.W., clartfy the structure and relationships of K. rasea and

RK. palycoelioides, and show that Cirrnlicarpus ynstrafiy and Meredithia nana are one species

how known as Cirrulicarpus nana (I.Ag.) comb. nov. Callephyllis coccinea is now referred to

as C. rangiferinns (Turner) comb, nav.

Introduction

Since the monograph of Womersley & Norris

(1971) on Australian Kallymeniaceae, further

SCUBA collections by S. A. Shepherd from

New South Wales and Tasmania have provided

material permitting clarification of some doubr-

ful species, and an earlier name for Callaphyllis

coccinea is evident,

1. Kallymenia cribrogloea Womersley &

Norris. 1971: 7, figs. 6-12, 78-80.

The range of this species was previously

given as from Waldegrave I., Eyre Peninsula,

5. Aust. to Port Phillip Heads, Vic, and Bruny

L,, Tas. Well developed, typical specimens have

been found in Jervis Bay, N.S.W., 18 m deep

in the southern end of the bay (Shepherd,

15.viii.1972; ADU, A42614). This extends the

range considerably, and SCUBA collections

from deep water may show that this is not an

uncommon species, though rarely found in the

drift because of its delicate nature,

2. Kallymenia rosea Womersley & Norris

1971: 9, figs. 13-18, 81, 82.

This specics was described largely on

numerous specimens of Lucas from N.S.W.

(mainly in NSW and MBL), collected before

1912; the enly other record was one specimen

from Port Stephens, N.S,W., in ADU,

The range of K, rosea can now be extended

to Jervis Bay in southern N.S.W. where it was

found 18 m deep in the southern end of the

bay, in sheltered situations (Shepherd, 15 viii.

1972; ADU, A42615).

This material (4 specimens) agrees well in

form with the Lucas plants but is without sut-

face proliferations and is medium red in colour.

Tr is slightly rubbery when fresh und fairly thin.

The thallus of liquid preserved specimens is

(150-) 250-300 um thick (rather more than

previously estimated from dried material) and

has ao epidermis of fairly compact cells prad-

ing rapidly to large, thin walled, ovoid, inner

cells with large intercellular spaces (especially

in the centre of the thallus); fairly loose,

moderately coarse, filaments are produced from

the larger cells (Fig. 1), Some of the large cells

become stellate, as previously figured ( Womers-

ley & Norris 1971, fig. 14).

Carpogonial branch systems ate polycar-

pogonial with 8-16 carpogonial branches, the

first cell of which is clavate to lobed, and the

second cell smaller and elongate; auxiliary cell

systems dre as previously described and figured,

but the large, ovoid, cell recorded as associated

with the carpogonial branch systems was not

apparent in the Jervis Bay material. Apparently

this cell is only a yegetative cell appearing

somewhat distinctive in the Lucas specimens.

Apart from young fusion cells, stages of carpo-

sporophyte development. were not present in

the Jervis Bay matcrial.

K. resea is probably a fairly deep water

species and is distincr from other Australian

species of Kallymenia in its farm, and from

* Depurtment of Botany, University of Adelaide Adelaide, $. Aust. 5001.

254 H. B. S. WOMERSLEY

oo’ 9089 Le SANT: 090 oyeceoason0gs ee?

eo ge Oe aes ASO

OO DSSDBNDO

100.um 7

Figg 1,2,3,4

Kise @H00G0 09000 08

50 um

Tes. 4a7 OD oe

AUSTRALIAN KALLYMENIACKAE

other similar foliose species in the presence of

polycarpogonial reproductive systems.

3. Kallymenia polycoelioides J, Agardh

1576) 687,

Meredithia palycoelioides (J.Ag.) J. Agardh

1892: 76; Womersley & Norris 1971: 42,

fig. 108.

Thallus complanate, foliose-subdichotomous,

ia 12 cnr high, ansing from a short stipe

1—+ mm long with a discoid holdfast 1-3 mm

across; thallus cuncately to broadly expanded

to 1-4 cm across at a few em above the stipe.

developing subdichotomous branches 1-14 cm

broad, and 1-2 cm between dichotomies, with

braad, rounded apices or lobes 3-6 mm across!

in some plants new subdichotomous fobes arise

proliferously from older basal parts. Colour

deep red to brownish-red, substance fairly soft,

adhering closely to paper on drying,

Thallus 400-600 pm thick (Fig. 23, with a

cortex 5-7 cells thick and a broad medulla of

fairly loosely arranged filaments mestly 7-15

utvin diam.; outer cortical cells fairly compact,

24 ym across and isodiametric in surface

view, inner cortical cells large: medulla with

stellate cells (Fig. 3) often with numerous arms

and slightly to moderately staining.

Curpogonial branch systems (Figs, 4, 5)

Monocarpegonial, the supporting cell lobed and

bearmg usually 4 lobed subsidiary cells and a

3 celled carpogonial branch, the first cell of

which ts lobed and the second elongate, Fusion

cell lobed (Fig. 4), Auxiliary cell systems (Fig.

7) relatively smal!, 25-50 ,.m across, consisting

of an auxiliary cell bearing about 8 subspherical

subsidiary cells each of which often bears one

further cell, Cystocarps scattered, about 2 mm

im diam. (in the type).

Male and tetrasporangial thalll unknown.

Type Locality—Orford, Tas. (Meredith).

Type—Herb. Agardh, LD (24843).

Disiribution,—South-eastern Tasmania. As

well as the lype, two fttrher Tasmanian

collections are known—Fluted Cape, Bruny

1 230 m (Shepherd, 121.1972; ADU,

A41925). and Great Taylor Bay, Bruny 1.

255

Previously this species was considered of un-

certain status {Wormersley & Norris 1971, p.

42) bur two collections by S.A. Shepherd from

near the type locality, and agreeing very well

in form with the type, show typical kally-

meniaceous female reproductive systems.

K. polycoelioides differs from other Austra-

lian species of the genus (see Womersley &

Nomis 1971, p. 4) in its subdichotamous habit,

and is most closely related to K. reba Womers-

ley & Norris in its structure and reproduction.

K. polyedelioides agrees well with Kally-

menia in thallus structure and in teproduction,

but differs from most other species in being

broadly subdichotomous (as in the holotype

illusteated by Womersley & Norris 1971, fiz,

118} rather than foliose or foliose-lobed: How-

ever, Codomier (1971) has referred two

Mediterranean species, which show 4 branched

habit. 10 Kallymenia, though without know-

ledge of the reproduction of either; K. pareny

{J.Ag.) Codomier becomes subdichoramous

several times, while K. spathulata ().Ag.)

Codomier is broadly furcate and lobed above,

K. polycoelioides has a fairly soft thallus,

drying thin and closely adherent to paper. and

not ¢arlilaginous, The texture, structure and

reproduction agree so well with other species of

Kallymeniga that K. polycoelloides cannot be

separated generically simply on the basis of its

habit,

Placement of K. potyevetioides in Kully-

menia involves consideration of the diflerence

between Aallynienia and Cirrulicarpus. The

latter is usually distinguished by its branched

thallus, Both the type species of Cirrulfcarpus

[C. gntelini (Grunow) Tokida & Masaki] from

Japan, and C. anstralis Womersley & Norris

(sce below) from southern Australia, have

thalli with several subdi- to polychotomous

branchings. While K. polycoelivides and Cirru-

licarpus both have a branched habit, the thallus

texture of the former is soft and not cartila-

ginous (as is typicul of most species of Kally-

menia), in contrast to the thallus of Cirruli-

carpus Which is cartilaginous, not or only

slightly adherent to paper, A possible distinc-

uon also lies in the cystocarps which Norris

25 m (Shepherd, 14411972; ADU,

A42131).

Fig 1. Kallymenia rosea. Cross section of thallus.

Figs, 2-7. Kallymenia polycoelioides. Fig. 2.—Cross sections of thallus with a stellate cel) and auxiliary

cel] system. Fig. 3.—Stellate cell. Fig. 4—Young carpogonia! branch system. Fig. 5—

Mature ¢arpogonial branch syslem, Fie. 6.—Fusion cell. Fig, 7, —Auxiliary cell system.

Abbreviations used: aux,c, auxiliary cell: sLe, stellate cell; subs.c, subsidiary cell; tr, trichogyne. f, 2, 3

refer to the first cell, second cell, and carpogonium of the carpogonial branch respectively.

236

et al, (1960) report as being compound or can-

fluent in €, pmelini, and which are grouped in

C. auxtrdis. For the present Cirrudicarpus is

best maintained as a distinct genus, but further

studies of distinctions between it and Kally-

menia are needed.

4. Cirrulicarpus australis and Meredithia

nana.

Womuersley & Norris (1971, p. 42) regarded

Mereatithia nana J. Agardh as of doubtful affi-

nity, commenting that the thallus structure is

kallymenivid but reproductive systems were not

geen adequately in the type. It was considered

that it might nol be a member of the Kally-

Mmeniaceac,

Further study of plants of Cirrulicarpus aus-

tralis Womersiley & Norris, especially of small

thalli, show that the type specimen of Mere-

dithia nana is almost certainly a young plant

of C. australis, Their form is comparable tak-

itig regard of the slate of development, the

structure in cross sectional view is identical.

and the type locality of M. nana (Port Phillip,

Vic.) is similar to that of C_ australis (Port

Phillip Heads).

The species should therefore be known as

Cirrulicurpus nana (J. Agardh) comb. nov,

{Basionym Meredithia nana J, Agardh 1892,

p. 76), with C. australis Womersley & Norris

(1971, p. 19, fizs, 39-43, 90) as a synonym.

H, B.S, WOMERSLEY

5. An earlicr name for Callophyilis coccinea

Harvey.

Since the publication of Womersley.& Norris

(1971), the lype specimen of Fucits rangi-

ferinus Turner has been examined. This speci-

men in the British Museum, from Kents

Islands, Bass Strait, was collected hy R. Brown

(No, 256) in 1803-4, und is a tetrasporangial

specimen 4-6 cm high, much branched with

slender ultimate branches typical of Callo-

phivllis coecinea Harvey,

‘The carrect name is thus Callophyilis rangi-

ferinus (Turner) comb, noy, (Basionym Fucus

rangiferinus Turner 1811, p, 114, pl. (83).

Following the original description of Turner,

F. remgiferinus was placed under Chondria by

C. Agardh (1823, p, 359) and under Aypnea?

by Greville (1830, p. hx) and Kuetzing (1849,

p. 761). J. Agardh (1852, p. 636) referred it

to Lecithites, but later (1876, p. 572) referred

his 1851 deseription to Mychodea harmuta

Harvey, excluding the previous synonyms. De

Toni (1897, p. 264). followed J. Agardh.

Acknowledgments

Loan of the type of F. rangiferinuy from the

Department of Botany of the British Museum

is gratefully acknowledged. Technical assist-

ance is acknowledged under a grant from the

Australian Research Grants Committee. | am

grateful to Professor R. E, Norris for com-

ments on the manuscript,

References

Pt 2, pp. 169-531,

Aqcaron, J. G. (1852).—"Species, Genera et Or-

dines Algarum". Vol. 2, Pt. 2. pp. 337-720.

(Lund).

Acaron, J. G. (1876).—"Species, Genera et Or-

dines Algarum”. Val. 3, Pt. 1, pp. 1-724.

Fpicrisis systematis Floridearum. (Lund, )-.

Acarpe, J. G. (1892).—Analecta algologiea. deta

Univ, lund. 28, 1=182, Plates 1-3.

Copomier, L,, (1971).—Recherches sur les Kally-

meénia (Cryptonemiales, Kallymeniacees), 1,

Les especes Mediterraneennes. Vie Milien 22,

ser. A. 1-54,

De Torr G. B, (1897),—‘“Sylloge Algarum om-

nium hucusque Cognitarium,” Vol 4

Florideae Sect. 1, pp. 1-388 (Padua.).

Grevitis, R. K- (1830) —"Algae Britannicae.”

(Edinburgh. ).

Kurrzinc, F. T,

(Leipzig, )-

Norns, R. E.. Toxma, J., & Masaxr, T. (1960) —

Fucther studies on Cirrulicarpus gmelini

(Grunow) Tokida et Masaki, Bull. Fac, Bish,

Hokkaido Univ. 11, 29-36,

Torver, D. (9811).—"Fuci sive Plantarum

Fucoram Generi a Botanicis Aseriptarum

Teones Deseriptiones et Historia.” Vol, 3, pp.

1-148, Plates 135-96,

Womenscey. H. B. S., & Norris, R. B. (1971).—

The morphology and taxonomy of Australian

Kallymeniaceae (Rhodophyta), Aust, J. Rot.

Suppl. Ser. No. 2, 1-f2

(1849),.—"Species Algarum,"

AMIDOSTOMATINAE (NEMATODA: TRICHOSTRONGYLOIDEA) FROM

AUSTRALIAN MARSUPIALS AND MONOTREMES

BY PATRICIA M. MAWSON*

Summary

MAWSON, PATRICIA. M. (1973). -Amidostomatinae (Nematoda: Trichostrongyloidea) from

Australian marsupials and monotremes. Trans. R. Soc. S. Aust. 97(4), 257-279, 30 November, 1973.

This work is a revision of the genera Austrostrongylus Chandler and Nicollina Baylis. Two new

genera are proposed, Paraustrostrongylus and Woolleya; these four genera, with Patricialina Inglis,

belong to the Amidostomatinae. Filarinema Ménnig is transferred to the subfamily

Mackerrostrongylinae. Austrostrongylus and Paraustrostrongylus spp. are recorded from a

phalanger and from macropod marsupials, Nicollina from monotremes and the numbat (a dasyurid),

and Woolleya from dasyurids and a native eutherian, the water rat.

New species described are Austrostrongylus hypsiprymnodontis from Hypsiprymnodon moschatus;

A. paratypicus from Macropus rufogriseus; A. chandleri from Macropus bicolor and

M. rufogriseus; Paraustrostrongylus bettongia from Bettongia cuniculus; P. trichosuri from

Trichosurus vulpecula; Nicollina calabyi and N. inglisi from Myrmecobius fasciatus; Woolleya

sprenti from Dasyurus viverrinus, Antechinus stuartii, Dasyurops maculatus and Thylacinus

cynocephalus; W. hickmani and W. monodelphis from Antechinus stuartii; W. martini from

Antechinomys spenceri.

Species redescribed in whole or in part are Austrostrongylus macropodis Chandler, A. wallabiae

Johnston & Mawson, A. aggregatus Johnston & Mawson, A. minutus Johnston & Mawson,

A. thylogale Johnson & Mawson, Paraustrostrongylus potoroo (Johnston & Mawson) (syn.

A. potoroo), and Nicollina echidnae Baylis.

Other new combinations are Woolleya sarcophili (Cameron), W. cathiae (Inglis), W. iota

(Mawson), W. acinocerus (Mawson), all transferred from Nicollina, and W. hydromyos (Mawson),

transferred from Austrostrongylus.

AMIDOSTOMATINAE (NEMATODA: TRICHOSTRONGYLOIDEA) FROM

AUSTRALIAN MARSUPIALS AND MONOTREMES

by Parricia M. Mawson*®

Summary

Mawson, Parricta M. (1973)—Amidostomatinae (Nematoda : Trichostrongyloidea) from

Australian marsupials and monotremes. Trans. R. Soc. S. Aust, 97(4), 257-279, 30

November, 1973.

This work is a revision of the genera Austrostrongyluy Chandler and Nicollina Baylis. Two

mew genera are proposed, Puraistrestrongylus and Woolleya; these four genera, with Palricia-

lina Trelis, belong to the Amidostomatinae. Filarinema Ménnigz is transferred to the subfamily

Mackerrostrongylinae. Anstrostrongylas and Parcustrostrongyluy spp, are recorded ftom a

phalanger and from muacropod marsupials, Nicollina from monoiremes and the numbat (4

dasyurid), and Wwalleya from dasyurids and 4 native eutherian, the water rat,

New species described are Austrostrangylus hypsiprymnodontis from Hypsiprymnedon

moschaius; A, paratypicus from Macrapuy riefogriseus; A. chandleri from Macropus hicelar

and M, rufogriseus; Paraustrostrongylys bettongia from Bettongia cunienlus; P, trichosuri trom

Trickosurus vulpecula; Nicollina calabyi and N- inglisit from Myrmecohius fasciatus; Woolleya

sprenti from Dasyurus viverrinus, Antechinus stuartii, Dasyurops maculatus and Thylacinus

epnocephalis: W, hickmani and W. monodelphis from Antechinus stuartii; W. martini from

Antechinomys spenceri.

Species redescribed in whole or in part are Austrostrangylus macropodis Chandler, A.

wallabiae Johnston & Mawson, A. averegatus Johnston & Mawson, A. minutus Johnston &

Mawson, A. thylogale Johnson & Mawson, Peraustrostrongylus potoroo (Johnston & Mawson)

(syn. A. poloreo), and Nicollina echidnae Baylis.

Other new combinations are Woolleya sarcophilé (Cameron), W. cathiae (Inglis), W. iota

(Mawson), W. déinocertts. (Mawson), all transferred from Nicollina, and W. hvdramyos

(Mawson }, transferred from 4 ustrostrengylus.

Introduction

The trichostrongyloid nematodes from Aus-

tralian vertebrates were discussed by Inglis

(1966) who considered that all belong to the

family Amidostomatidae. In the subfamily

Amidostomatinae he included (from marsu-

pials) the general Filarinerma MGnnig, Patricia-

lina Inglis, Anstrostrongylus Chandler and

Nicollina Baylis. Filarinema, however, differs

markedly from all other genera of the sub-

family in the virtual absence of a buccal cap-

stile—the teeth occur in an enlargement of the

anterior end of the oesophagus, so this genus

should be referred to the subfamily Mackerra-

strongylinae Inglis, in which a buccal capsule

is absent. Of the three genera from mono-

tremes and marsupials remaining in Amido-

stomutinue, no Parrictalina sp, has been found

during the present study,

Up to the present, most of the species from

marsupials have been identified as belonging

to either Austrostrongylus (type species A.

macropedis Chandler, 1924) or WNicollina

Baylis, 1931 (type species N. tachyglossae

Baylis, 1930), Proposing the genus Nicollia

(which he changed to Nicollina in 1931)

Baylis stated that this genus differs from

Austrostrongylus in the presence of a shallower

buccal capsule, the symmetrical bursa, the ab-

sence of ventral teeth, and in the shape of the

tail of the female. More species were later attri-

buted to each genus, and Mawson (1960, p.

264) pointed out that among species with ven-

tral teeth, the female tail in some: is conical

and in others bears a terminal spine, and it was

suggested that the best character on which to

separate the gcncra would be the shape of the

spicules, which in Avstrosirongylus spp. are

* Zoology Department, University of Adelaide, Adelaide, S. Aust. 5000.

15%

entire and in Nicollina spp. are bilid or trifid

distally, Inghs (1968, p. 336) agreed with this

and pave an amended list of species belonging

to each venus.

In the present study, 13 new species of ani-

dostomes haye been identified from maono-

wemes und from 4 variely of Australian mar-

supials, inzioding, dasyurids, from whith only

oie species had previously been described (N.

caihiae Jaglis, 1968). The identification of

these hus entailed the re-examination of all

available puratype or holotype specimens of

existing Species, and uw re-evaluation of the

generic characters.

Discussion

Two qew genera are proposed, Paraurtro-

iromgylus nd Woeolleva. Both Parausiro-

strongylus spp. aid Ausrrostronyyhey spp. are

characterised by wide and thick lateral alae and

and single-tipped spicules, and these features

distinguish them from Nicelltna spp. and

Woolleva spp. in which lateral alae if present

are small aod thin and the spicule tips are

divided, Distinct differences in the form of the

buceal capsule and dorsal looth distinguish

Nicollina app, trom Woalleya spp, These tour

genera are found in different hosts, A itra-

srrongvlus spp. and Paranstrosivengylus spp.

‘being recorded fram macropods and phalangers

(herbivores), Nicellina spp. from the echidna

und the numbat (termite and anteaters} and

the platypus. (which eats worms, etc.) and

Woolleya spp, Crom dasyurids, bandicoots, and

a eutherian, the water rat Call camivores),

However, there are some species which are

not satisfactorily accounted for Lhe spicules

of A. cameroni (Mawson), W. sarcophilt

(Cameron) and W, acinocercus (Mawson) are

not divided, but the body lacks the lateral alae

utd the characteristic bursa of Anstro-

virenoryins and Paruusirestrongylus,. In Waol-

leva nnvnodelphiy musp. and BO hydromyes

(Mawson) the spicules are divided and the

loneitiidinal crests are like those of Woolleva

spp. hut the tail of the female is pointed and

lacks a spine. The position of these species will

be discussed under Woulleya nig.

‘The characters of the four venera will be

described in detail below, but some general

remarks are made here about the cuticular

swellinis and crests commonly found in species

of all these genera. Cuticular ridges and cuti-

cular inflations in the Heligmosamatidae have

been studied in detail by Durette-Desset (1964,

|966) in species {rom the Old and New

Worlds, According to this author almost all the

PATRICIA M. MAWSON

heligmasarnes are rolled into a sinistral spiral.

Some live coiled around villi (with the anterior

end wwards the base of the villus) und main

tain their position by a combination of pinch-

inz with the internal (best devcloped) crests

uod the apposition of lateral crests and glae

Others, in which different arvas of the body

beur the best-develuped crests. also form a

sinistral coil, but not around a villus, and these

move through the mucus between the villi with

« corkscrew action, so |hat the outside of the

coil (the dorsal body surface) which bears the

best-leveloped crests, comes in contact with

the villi.

Although they belong to a different group

from the Heligmosomatidae, the Australian

amidostomes muy be compared with them itt

yome respects, If they wre cuiled, it is in a

sinistral spiral. Im some genera 4 4¢atro-

strongelus and Paraustrostrongylus) the Sateral

afag are Very well developed, not only out from

ihe body in a lateral direction, bul they are

wlmost 2s thick, dorsoventrally. as the body

(Fivs. 7, 13, 26). The cuticle over these en-

larged alac bears one or more Jongitudimal

ridyves, and there are alsa one of morc crests

on the ventral surface of the body proper,

These alae differ from those described by

Durelte-Desset as enlarged crests, because the

enlargement is caused by subeuticular swelling,

the crests themselves being of normal size (as

indicated by their cuticular “skeleton") and

merely borne on the inflated cuticle. In other

genera, Nicollina and Woolleya, lateral alae are

less distinct, and the loneitudinal crests are

variously distributed, In all cases males and

females of the sume species show similar pecu-

liarities of structure and distribution of the

erests. In some species, but hy no means in all,

there is 4 Bradient "round the bady jn the size

of the crests. In many Australian species, crests

are ohbsent on the dorsal surface. An attempt

has heen made to classify the various specics

according to alae and crests. Those with twa,

wide, thick lateral alae form a natural group

(also distinguished by other characters) which

is further differentiated into the two genera

Austrostrongylns and ~~ Paraustrostronyylus.

Among the remaining spectes, in which lateral

alae if present are of a different type, longi-

tudinal crests are variously arranged-- they may

be many (8-20 of more) and distributed all

round the body, or they may be few (2-4), and

restricted to the ventral surface. However,

acither of these types 38 associated with any one

of the lypes of spicule tips, dorsal ray or female

AMIDOSTOMATINAR FROM AUSTRALIAN MAMMALS 239

tail, so that further classification op the type

of crests is impracticable.

Most of the specimens cxamined were nol

seen jn situ in the host, although a few were

found coiled round torn off villi,

Unless otherwise jidicated, all the trans-

verse sections figured Were taken about the

rudhody of the worm

Measurements of new material are given in

Tables 1, 2, 3, or 4, as indicated in each case

iinder the species heading. Types of new spe-

cies Will be deposited in the South Australian

Museum, Adelaide.

Key to genera

|. Latera| alac wide and thick; dorsal Jobe of

hursa markedly thickened 2

1. Lateral alpe, if present, thin; ‘dorsal Jobe of

bursa fot thickened

2. Genital cone well developed, ‘hitinised

Paranstrosironyy lias

2. Genital cone not well developed, not chiti-

hised Alistrastrongylus

3. Buces! capsule a shallow ting; dorsal ioath

hhunt, protrusible ., _.. Nivallina

Buccal capsule # domed anteriorly: darsal tooth

pointed Weolleya

AUSTROSTPRONGYLUS Chandler

Amidustomatidac: Small usually coiled worms

with thick «nd wide Jateral alge: Jonzitudinal

cuficuJar crests on alae aml on body proper:

cephalic cuticle inflated; buccal capsule well

developed, with one dorsal and sometimes twa

smaller subventral oesophageal teeth. Male:

bursa more or less symmetrical, lateral lobes

long, dorsal short and thick; dorsal ray usually

dividing into three pairs of branches; externu-

dorsal ray arising separately, other rays from

same root, separating al tips; genital cone not

distinct, spicules slender with simple points,

sometimes united by small alae. Pemale: tail

tapering to long point; vulva heur posterior end

of body, ovejectors divergent, Parasites of

small intestine of macropod marsupials,

Type Species: od, macropodis Chandler,

1924: 160,

Other species: A. ageregatus Johnston &

Mawson, 12406: 472; 4A. minutes Johnston

& Mawson, 1938; 195; 4. rhylogale John-

stan & Mawson, 1939: 534; 4, paratypicus

nap., 4. chandleri nsp.; A. hypsiprymnodon

TSP.

In some species of Austrusirurgy lus, perhaps

in all, there is a strong tendency to {he deposi-

tion of a dark reticular and granular material

under the cuticle. Durette-Drssel (1966, pp.

457, 461) notes a similar conditiun in same

heligmosomes and. hy staining, concluded that

sul lobe obscures the final branching

it is a chitinnid subslance. This occurs espe-

eially in the lateral alac aud if the bursa, and

sometimes in the cephalic inflation, but may

also appear in the older female between vulva

and anus, all round the bawdy. The distribytion

in the bursa appears to vary with the species;

in many cases it obscures the dorsal ray, espe-

clally in jong- stored specimens: it is resisten

to clearing in lactophenol, but less so in creo-

sote or Berlese's Fluid.

Tn all species of Austrostrongylus the dorsal

lohe of the bursa, whether containing granular

material or not, is: much thickened, so much so

that the lohe is in fact almost spherical, the

inner or ventral face of the lobe extending to

the cloaca, A genital cone, as such, is absent.

Because of the shape of the bursa, the dorsal

ray must be considered in three dimensions

Tather than two.

The characteristic bursa, and the striking

strap-like form given to the body by the wide

thick alac, appear to be important diagnostic

features of the genus, allhough they have not

previously been mentioned. Both characters

are present in the type species of the xentis,

which is partially redescribed below,

Austrostrongylus macropodis Chandler, 1924:

160, From Bennett's Kangaroo, Macropus

rufogriseus var, bennetti,

FIGS. tf, 2

The type and paratype material of A. praero-

podis fas been examined, The holotype male

and cotype female (U.S.N.M- Helm. Call.

26124) are va slides and impossible to exa-

mine thoroughly. What is assumed to be the

piralype material is in the collection of the

Department of Biology, Rice University. This

material (H,N. 23049) is. labelled ‘from Ben-

nett's Kangaroo’ and was worked on by Dr.

Chandler. The specimens agree closely in most

particulars with Chandler's description af 4.

mocropodis. They have the wide Jateral alac

and the swollen dorsal lobe of the bursa which

have been seen in all other species of the

genus. Unfortunately the darkening of the dor-

of the

dorsal ray. It is clear, however, that the dark

part of the dorsal jobe extends nearly to its

posterior border, and that my Chandlec’s Vig. 3

the clear part of the lobe is its swollen inner

surface, which is unpigmented. afd which in

some positions of the bursa appears to be its

posterior border. Thus the dorsal ray extends

nearly to the posterior edge of the bursa, and

the dorsal lobe is shorter that) indicated hy

Chandler. There may he two or three pairs of

branches of the dorsal ray. but the tips of the

inner branches shown here in Fig, 1 are not

clear. If there are only two pairs, this is the

only species of the genus in which this is so.

The tips. of the spicules are enlarged by alae,

as figured by Chandfer.

The bodies of these specimens ure so much

contracted thai a good transverse section could

not be drawn, Allowing for some distortion,

the sections made show alae and crests similar

to those shown in Figs. 14 and 18, but with an

extra crest on the dorsal aspect of the right

side,

Key to species of Austrostrongytus

|. Female nvonedelphou. 4. rypeipremepdants

1. Female didelphous

2. Vagina lang, more or tess equal to distance

from vilvu lo anus A. aguregaius

2 Vagina short

Splewles with rehitively wide alae round tips 4

Spictiles with small or no alae at tips... 5

4. Male 45-5 mm Jong, spicules 375-500 «wm

A. macrapodis

4+. Male 3,8-4.7 mm long, spicules 520-700

ain . A, paratypicus

§. Dorsal ray gives off first pair ‘of branches, then

bifurcates ; A, minutes

5, Dorsal ruy gives off two pairs of branchex,4 then

bifurcates rie at

6. Tips of spicules united in small ala... . 7

6. Tips of spicules not united in ala

A, wallabfae

7, Three crests on each Isteral ala; branches of

dorsal tay elongate... . A, thylagale

7. One crest on each | lateral ala; branches of

dorsal ray short, stout A. chandleri

Austrostrangylus wallabiae Johnston & Maw-

son, 1939: 534, from Macropus mufrogriseus

(syn. M. ruficollis).

FIGS. 3-6; TABLE i

Host and locality: Macropus rufogrisens from

Logan Village, Qld.

New specimens a* well as the type material

have been examined and the original descrip-

tion can now be amended. As was stated. the

type specimens are darkened by masses of

granular material deposited under the cuticle

in the wide, thick, Jateral alae, in the bursa,

especially in the dorsal lobe, and in the female

al the posterior end of the body—in a few of

the older specimens this tegion is so distended

as to overhang the anus. In the newer speci-

mens from Qucunsland there are similar dark

masses biti these are neither so thick nor so

dark.

On the broad lateral alae there are longi-

tudinal crests, three on one side, two on the

other: there are wlgo two large and one small

ventral crests, There are no dorsal crests except

those on the dorsal side of the alae (Fig 1),

hed Nand

PATRICIA M. MAWSON

In the feniale the lateral alac terminate at about

the level of the vulva, in the male the left ala

reaches nearly to the bursa, and the right

rather shorter,

The buccal capsule is well developed with

two small ventral, and one large dorsal, teeth,

The spicules are very slender, with simple

acicular tips not enclosed in alae. The bursa is

thick-walled, especially the dorsal Jobe, and is

more or less symmeirical—in some specimens

the right lobe is rather longer and narrower

than the left. The dorsal ray, seen more ¢learly

in the new material, has one more pair of

branches than origitrally described (Tig, 4).

The vulva in the original material 1s 500-600

pmo. from ihe posterior end of the worm (not

1,500 pm). The cuticle just in front of the

vulva is more or Jess inflated (Fig. 2).

Although the species is similar to A. macro-

podis, there are distinct differences in the bursal

rays, and there appears to be less granular

miaterial deposited in various parts of the bady,

Austrostrungylus aggregatus Johnston & Maw-

son, 1940; 472, from Wallabia bicolor (syn.

Macropus nellahatus).

FIGS, 7-10; TABLE |

Host and locality: Wullahia bicelor

Logan Village, Old.

The type male und female and the paratype

material of this species have been re-examined

and compared with the new material. Measure-

ments of the ncw matertal are given in Table |

Two asymetrical laleral alae are present, a3

well as. three ventral longitudinal crests. The

oesophagus widens gradually in its posterior

third.

The vagina is unusually long, reaching a

distance anterior to the vulva about equal to

that of the vulva from the posterior end of

the body,

The bursa is thick, particularly the dorsal

Iohe, and darkened with 4 granular deposit. In

one male this deposit is almost absent. and

the branches of the dorsal ray quite clear (Figs,

8, 9). The spicules. are long and very slender,

hoth ending in one als. The pobernaculum is

4 thin plate.

from

Austrostrongylus minutus Johnston & Mawson,

1938: 195, from Macrepus dorsalis.

FIGS. 11-12

The paratype inaterial of this specws has

been examined; the lateral alae and the dorsal

Iohe of the bursa agree with the revited delim-

tion of these sinictures in A ustrostroniyyitey.

However, the few specimens have been greatly

Figs.

Figs,

Figs.

3-6,

7-10.

11-12.

13, 14.

AMIDOSTOMATINAE FROM AUSTRALIAN MAMMALS 261

i iledith Lies macropodis. Fig, 1.—Posterior end of female, Fig. 2—Posterior end

of male.

Austrostrongylus wallabiae. Fig. 3.—Transverse section of body of female. Fig, 4— Pos-

terior end of male. Fig. 5.—Dorsal ray. Fig, 6.—Posterior end of female.

Austrostrongylus aggregatus. Fig. 7,.—Transverse section of body of male. Figs. 8 and 9.—

Lateral and yentral views of dorsal ray, Fig, 10.—Posterior end of female.

Austrostrongylus minutus. Fig, 11.—Lateral view of dorsal lobe and dorsal ray. Fig,

12._Ventral view of dorsal ray.

Austrostrongylus thylogale. Fig. 13.—Transversc section of the body, Fig. 14.—Laterail

view of dorsal lobe, with dorsal and one externo-dorsal rays,

Figs, 3, 6, 7, 8, 11 and 13 to scale beside 6: Figs. 9, 12 and 14 to scale beside 12.

242

flittlened abd a useful transverse section can-

not be given. There appears to be only one

ventral hody crest, apart from those on the

alae, The lateral alue extend beyond the vulva

in the female, and in the male the left ala is a

little longer than the vight. The right side of

the bursa is rather longer than the left, but the

rays are similar on the two sides, The dorsal

lohe is so swollen as to be almost spherical,

and the three pairs of branches of the dorsal

ray (not two pairs) lic wlmost at Tight angles

to its main pxis.

Austrostrongylus thylogale Johnston & Maw-

gon, 1940a: 99, from Maeropus engenit

(syn. Thylogale eugenii), from Kangaroo 1,

5. Aust.; Mawson, 1959: 155, from Setonix

hrachyura, trom Rottoest I, W, Aust.; Inglis,

19OR! 336, from S. brachvura. W. Aust.

PIGS. 13-14

Specimens from the Kangaroo I. wallaby

have becit studied and compared with those of

other species ol Austrostrongy/us. The Jateral

alae wre broad and wide, asyoumetrical in sec-

tion, With three asymmetrical crests on the alac

and Wo Ventral crests on the body.

A. thylogale appears to be free from: the

granular Ucposits which obscure, or partially

obscure, the bursa uf some other species of the

genus, The swollen dorsal lobe of the bursa is

clear, and in it can be seen the three pairs of

branches of the dorsal ray, penetrating the lobe

in three planes (Fig. 14). In the female the

{aternl alae extend to just behind the. vulva; in

the male the left continues nearly to the bursa,

the right ends shortly anterior to this. The. spi-

cule fips are united in a very small ala.

Anstrosirongylys paratypicus 0.sp.

Fas. 15-18. TABLE |

Host anu localitys Marropus rufogriseus from

the Bathurst district. N.S.W

In the same host animal us specimens of

Austrestrangylus wullabiae, there were ubout

20 specimens of a smaller and apparently new

Austrostrongylis sp. The body form is similar

to that of 4. wallabiae, more or less tightly

cotlecL The Jateral alae are very wide, wilh one

crest on the lett side and two on the right, and

there ure in addition two ventral crests. ‘To-

wards the posterior end of the male the Icft

ala terminates. but the right, in most specimens

dark with granular material, continues nearly

to the fursa. In the female, the lateral alue

extend to or a little beyond the vulva.

The buccal capsule is well developed, the

dorsal tooth larze and the two sub-ventral teeth

PATRICTA M. MAWSON

small, The nerve ring surrounds the oesophagus

towards the end of the second third of its

length. The excretory pore is close to, oF

behind, the buse of the oesophagus in the mele,

rather More anterior in the female.

The tail of the female tapers to a Jong cylin-

urical process, Hoth ovejectors are well deve

loped, A ulerine egg near the ovejector m& 90 x

45 pm.

The bursa is thickened with granular mate-

Mul, especially in the dorsal lobe, where 2 offen

obscures the detail of the dorsal ray. The

lateral lobes. are asymmetrical, the let wider

than the nght. The three lateral aud twa ven-

tral rays are closer together in the right Yobe,

diverging only near their tips, The eaxterno-

laleral ray of the left side is distinctly larger

than that of the tight. The dorsal ray gives off

two branches before its finul bifurcation, Tot

all in the same plane (Fig. 18),

‘Vhe spicules widen near their distal ends; the

tips are wate, the alae are folded around the

lips when lying in the body and when dissesteu

out; in no case were the spicules extruded

naturally. The gubernaculum is very small andl

thin.

The species is distinguished from: A. walla-

biwe by the more posterior position of the

vulva, the shape of the spicult tips, and the

asymmetrical bursa. It seerns to be close to 4.

macrapadis (from the Vasmanian sub-species

ol Macrepas mafogrisexs). However, the spi-

cules are longer, Because of this and the appa-

reni difference in the branching of the dorsal

fay, and also because the hosts come from

widely different localities, the two species are

regarded as separate.

Austrostronpylus chandleri n.sp,

FIGS. 19-24; TABLE |

Hosts and localities: Macropus rufogrisens

(type host) from Waedlabia bicolar Tram

Lovun Village, Qld.

‘The body is loosely coiled. The lateral asym

metrical alae are well deycloped, each with one

crest; in addition, Iwo ventral crests ure pre-

sent. The buccal capsule is well developed, the

dorsal tooth about half the depth of the cupsule

und the two sub-ventral tecth smull.

The tail of the femule tapers, ending in a

thin finger-like piece. The vulva, Well in front

of the anus, leads to 4 short vagina; the ove-

jectors are about equal in sive. The cges are

75-R5 x 45-50 pm,

The spicules are long, slender throughout

their length, and end in blunt tips siightly

curved ventrally and.enclosed in a single small

263

AMIDOSTOMATINAE FROM AUSTRALIAN MAMMALS

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Figs. 15-18.

PATRICIA M. MAWSON

304m

Austrostrongylus paratypicus. Fig. 15.—Head. Fig. 16-- —Transverse section of body of

male. Fig, 17.—Posterior end of female. Fig. 18.—Bursa of mule.

Austrostrongylus chandleri. Fig- 19.—lead, Fig. 20.—Transverse section of body of male.

Fig. 21.—Posterior end of female. Fig. 22.—Lateral view of bursa. Fig. 23.—Ventral

view of dorsal ray. Fig. 24—Tip of one spicule.

Fies, 15, 19 and 20 to scale beside 20; Figs. 16, 18, 22 to scale beside I8; Figs, 23 and 24 to scale

Figs. 19-24.

beside 23.

oval ala. The gubernaculum is small and in-

conspicuous,

The bursa is more or less symmetrical, the

dorsal lobe thick, the genital cone absent as

such, The granular thickening of the bursa is

strongly developed, darkening much of it, in-

cluding the dorsal lobe and the area posterior

and dorsal to the externo-dorsal rays.

The species resembles 4, wallabiae in the

arrangement of the bursal rays (Figs, 22, 23).

It differs however in the distribution of the

granular material in the bursa, in the absence

of a lateral ala extending nearly to the bursa,

and in the shape of the tips of the spicules.

The form of the bursa and shape of the spicule

tips are close to those of A, thylogale, but in

AMIDOSTOMATINAE FROM AUSTRALIAN MAMMALS

this species the bursa is without granular inelu-

sions, the spicules are shorter, and the shape of

the dorsal ray is different.

it will be seen from the measurements given

in Table | that the specimens from H’. bicolor

are sinaller that: those from the type host.

There is also some difference in the position of

the longitudinal crests on the lateral alae in

gpecimens from the two hosts, although this is

similar in males and females for the same host,

and in collections from the same host species.

The value of this difference is uncertain; no

other morphological difference can be seen

heween the specimens.

Austrostrongylus hypsiprymnodantis n sp,

FIGS. 25-29; TABLE 1

Host and locality: Aypsiprymnodon moschatet

from Qtd,

This is.a small coiled worm, with very well

developed lateral alae, af which the right is

wider than the left. There are five longitudinal

crests, two on each Jatetal ala and one on the

ventral surface of the body. In the female the

right ala is a little shorter than the left, which

widens considerably before ending at ahout the

level of the vulva. In the male the two alac

extend from just hehind the cephalic inflation

nearly to the bursa, where they end abruptly

ut the same level,

The buccal capsule is well developed. The

dorsal tooth is ahout half the length of the

capsule. The exeretory pore lies well behind the

oesophagus.

The bursa is symmetrical, the dorsal lobe

short and swollen and with a vesiculale struc-

ture internally, which rather obscures the dorsal

ray, The arrangement of the rays is shown in

Figs. 28, 29. The spicules are long and slender

and end in a point, The presence of tenminul

alae could not be determined. A small guber-

naculum 18 present,

The tail of the female is about half the dis-

tance [rom vulva to posterior end of the body.

Only one, the anterior, uterus and ovejector is

present, Eggs wre 63-65 x 35-37 yum.

This species has been referred to Ansrro-

strorgylas because of the inconspicuous genital

cone, the origin of the externo-dorsal ray, and

the way whe lateral alae in ihe male end at the

same level just in front of the bursa. In these

features it differs from Paraustrestrangylus spp.

It is distinguished from other species of the

genus by the monodelphous condition of the

female and the posterior position of the vulva,

The cuticular swelling around the vulva is of

265

the irregular’ form seen im other species of

Ausvostenueylus rather then the definite ven-

tral owerowth seen in Parairtrostrangylur spp-

PARAUSTROSTRONGYLUS nz.

Amidostomatidae; Small, usually coiled, worms

with thick, wide lateral alae: longitudinal crests

present on alae and on rest of body; cephalic

inflation present; Ventral cuticle at posterior

cod of body inflated, forming prebursal, or pre-

vulvar, swellings usually of distinctive shape.

Buccal capsule small, with dorsal oesophageal

tooth, Ventral tecth present or absent. Male:

burs of two lateral and one small dorsal lobes,

thickened dorsally and usually ventrally; ex-

terno-dorsal ray arising from base of dorsal,

dorsal dividing into three pairs of branches,

ventro-venttal tay diverging markedly at its

base from latero-ventral and lateral rays;

genital cone strongly chilinised, spleules long

and slender, ending together in one or two alae;

guhernaculum small, plate-like; Female: tail

tapering to long point; monodelphous, only

anterior ovejector, uterus, and ovary developed_

Parasites uf the intestine of macropod mar-

supials.

Type species: P. potorac, syh. Aisitro-

strongyliy potoroa Johnston & Mawson,

1949,

This genus is close to Ausrtrostrongylus in

the form of the lateral alae, the swollen dorsal

lobe of the bursa, and the tapering tail of the

formale, It is distinguished trom it by the pre-

sence of a well developed genital cone, diver-

gent ventro-ventral rays in the bursa, and a pre-

borsal cuticular inflation in the male, and by

the absence of the posterior part of the repro-

ductive system of the female.

Paraustrostrongylus patoroo (Johnston & Maw-

son, 1969: 64), from Pororeus tridactylus.

FIGS. 30-33; TABLE 2

Host and locality: Pororous tridactylus from

Hobart; Tas,

The type material of this species, as well as

fresh material from the same hosl species, has

been examined and a fuller description is now

given,

The Jeft lateral ala is thicker than ihe nght;

each bears two crests, and in addition there are

two ventral cuticular crests and one dorso-

lateral on the right side, These crests com-

mence in the oesophageal region and continue

to about the level of the vulva in the femafe

and nearly to the bursa in the male, In the male

the Jeft ala becomes greatly inflated just an-

PATRICIA M, MAWSON

25-29. Austrostrongylus hypsiprymnodontis. Fig. 25.—Head of female. Fig. 26,—Transverse sec-

tion of body of male, Fig. 27.-—Posterior end of female. Fig. 28—Posterior end of

30-33. Purausirostrongyliy potorov. Fig. 30.—Transverse section of body of male. Fig. 31,—

Transverse section of male shortly in front of bursa. Fig. 32,—Posterior end of male.

Figs.

male, Fig. 29.—Dorsal ray,

Figs,

Fig. 33.—Posterior end of female.

Figs. 26, 27 and 28 to scale beside 28: Figs. 29, 30,

terior to the bursa: the right ala ends a little

anterior to this inflation. The subventral cuticle

on the right side anterior to the bursa is raised

into an elongate “blister” on which there are

three obliquely longitudinal crests (Fig, 31).

The buceal capsule is small and the dorsal

tooth relatively large. The ventral teeth are

very small. The nerve ring lies just behind the

mid-length of the pvesophagus and the excre-

tory pore is near its base.

The tail of the fernale tapers to a long point.

The cuticle anterior to the vulva is greatly en-

larged, forming a rounded mass overhanging

34, 32 and 33 to scale beside 32.

the vulva. The shape of this mass is similar on

all new specimens cxamined, from two hosts,

but in the older specimens il is flaltened. Only

the anterior part of the female reproductive

system is present.

The bursa is slightly asymmetrical, with the

left side, and its rays, a little larger than the

right. The thickening of the dorsal lobe is. not

very marked. The arrangement of the bursal

rays is shown in Fig, 32. Fhe spicules are

simple, undivided at the tips. A ‘small guber-

naculum is present. The genital cone is strongly

chitinised, and probably acts as an actessory

guide for the spicule.

AMIDOSTOMATINAR FROM AUSTRALIAN MAMMALS

267

TARLE 2

Measurements of Paraustrostrangylus spp, Waless otherwise indicated, meastirements ave itt pn:

I, petorso P. bettungia P. trichogurl

Male:

Length (mm) 2,4-2,6 4,0-4,4 4,3=5,3

QOesophagus 240-275 340-380 4350-421)

Ceph. inflation 40-48 70-80) 90-100

Antr.end—nerve ring 120-150 218-230) 250-270

—excr. pore 210-230 330-400 460-510

Spicules 250-260 380-400 380-450

Gubernaculum 4045 45-50) 35-40

Female:

Length (mm) 2,7-3,0 5.7-6.0 5.0-6.7

Oesophagus 250-290 340-41) 400-435

Ceph, inflation 45-50 80-85 80-1)

Ante. end—nerve ring 130-140 20-220 230-260

—exer, pore 200-250 280-340 440-510

Tail 90-120 105-140 120-150

Postr, end—yulva 450-200) 310-370 250-330

Paraustrostrongylus bettongia n.sp.

FIGS. 34-41; TABLE 2

Most and locality: Bettongia gaimardi from

Tas.

These are relatively large worms lying in

tight or loose coils, There are two longitudinal

crests on each lateral ala and two additional

ventral crests. Each of these ends a little in

front of the vulva in the female. Shortly in

front of the bursa.of the male, the right ala dis-

appears but the left is much enlarged. Between

the termination of the right ala and the bursa

there is an elongate subventral inflation beanng

3 to 4 oblique-longitudinal crests (Fig. 38).

In nearly every specimen the anterior end is

curved back against the rest of the body. The

cephalic inflation is about a fifth of the length

of the oesophagus. The buccal capsule is shal-

low, the dorsal tooth short. The nerve ring is

at about the middle, and the excretory pore

near the posterior end of the oesophagus.

All three fobes of the bursa are thickened.

Ventral to the chitinised genital cone there is a

cuticular thickening. which merges at each side

with the ventral part of the bursa, and which is

penetrated by the ventro-ventral ray, The

arrangement of the bursal rays is shown in

Figs. 39-41. Because of the thickening of the

dorsal lobe, the branches of the dorsal ray are

not all in the same plane, The spicules end in

alae, folded around the tips. The short guher-

naculum is finely bossed.

The vulva is about three tail lengths from

the posterior end of the body. Anterior to the

vulva the ventral cuticle is greatly inflated, and

hangs over the vulva in an elongate sausage

shaped mass, The shape of this mass is similar

in all specimens from the two host animals.

No vestige was seen of the posterior part of

the female reproductive system. Eggs are

54-55 x 32-33 pm.

The specics is distinguished from P. peforeo

by the form of the bursa, which is not asym-

metrical and is thicker-walled, by the size of

the ventral tooth, the distance of the vulva from

the anus, and the shape of the vulvar flap.

Paraustrostrongylus trichosuri n.sp.

FIGS. 42-47; TABLE 2

Host and locality: Trichosurus vulpeavla from

D’Aiguillar and Camp Mt., Old.

These worms are coiled into a fairly tight

spiral from which the anicrior and posterior

ends protrude, The lateral alae are well deve-

loped, the right with three longitudinal crests

and the left with two, and there are also three

ventral longitudinal crests. In the male the

crests and right ala disappear a short distance

in front of the bursa and ure replaced by a

sub-ventral inflation. The left ala is wider jn

ihis region and terminates close to the bursa. In

the female the alae and crests are discontinued

just in front of the yulva and there is a separ-

ate small ventral inflation just antcrior to the

vulva.

The cephalic inflation is about a fifth of the

length of the oesophagus. The buccal capsule

is shallow, and the dorsal tooth small; sub-

ventral tecth are apparently absent,

In the female the tail tapers to a fine point:

the vulva is about a tail length ta front of the

anus. Eggs are about 70 x 45 pin.

PATRICIA M. MAWSON

500m

Figs, 34-41. Paraustrostrongylay bettoneia. Fig, 34—Head of female. Fig. 35.—Transverse section of

body of male. Fig. 36.—Posterior end of female. Fig, 37.—Posterior end of mule. Fig.

38.—Transverse section of body through prebursal inflation. Fig, 39.—Ventral view of

bursa, without coverslip. Fig. 40.—Lateral view of bursa. Fig, 41,—Dorsul and externo-

dorsal rays.

Figs. 34, 35, 39, and. 40 to scale heside 40; Figs. 36 and 37 ta scale beside 37,

The margin of the bursa is entire, and the

dorsal and ventral parts are swollen. The geni-

tal cone is strongly cuticularised. The arrange-

ment of the rays is shown in Fig. 46. The

dorsal ray however is partially obscured in all

specimens examined by refractive inclusions

in the bursal wall close to the mid-dorsal line;

the ray is small, as it must be restricted to the

region of the inclusions.

The species. differs from both P. poterae and

P. betiongia in the greater development of

lateral alae in comparison with the hody dia-

meter, as well 2s in the dorsal ray and the

smaller prevulvar swelling. The bursa itself is

less swollen than that of P. bertongia and more

so than that of P. poterao.

NICOLLINA Baylis

Nicellina Baylis, 1930; 550, syn. Nicollia

Baylis, 1930, nec Nuttal, 1908, nec Krit-

schewsky, 1922.

Amidostomatinae: body with longitudinal

crests and sometimes with ofe or two Jateral

alac: anterior end with inflated cuticle; buccal

capsule shallow, stoutly built, containing a blunt

dorsal ocsophageal tooth. Bursa more or less

symmetrical, dorsal lobe absent or poorly deve-

loped; dorsal ray dividing into four branches;

externo-dorsal ray arising separately or from

base of dorsal ray; lateral and ventral rays

somewhate divergent. Spicules usually bifur-

cate or trifurcale; gubernaculum present. Fe-

AMIDOSTOMATINAER FROM AUSTRALIAN MAMMALS

Figs. 42-47, Paraustrostronyylus trichosuri, Fig. 42.—Head of male. Fig, 43.—Uransverse section of

body of female. Fig. 44.—Posterior end of female. Fig, 45.—Posterior end of mule. Fig,

46.

Bursa spread aut, inside view. Fig. 47.—Tips of spicules,

Figs. 43: and 46 to same scale, 44 and 45 to same scale, 42 and 47 to same scale.

male didelphous, vulva towards posterior end

of body; tail of female with dorsal terminal

spike and two short subveniral terminal lobes.

Parasites of monotremes and Australian mar-

supials.

Type species: N. tachyglossae (Baylis).

Other species: N, echidnae (Baylis, 1930);

N, ridei Inglis, 1969: N. camereni Mawson,

1959: N. calabyi nsp.; N. inglisi asp.; N.

baylisi n.sp.; N. mundayi asp.

Through the courtesy of Dr. W. G. Tnplis

and the British Museum (Nalural History) it

has been possible to examine the type speci-

mens of N. tachyglossae and N. echidnae. In

comparing these with other species attributed

ta Nicollina, it appears that not enough con-

sideration has been given to the shape of the

buccal capsule and the dorsal tooth. In N,

tachyglossae (Pig. 48) and N. echidnae the

buccal capsule is shallow, ring-like, and stoutly

built, and the dorsal tooth is blunt and

apparently readily protruded through the

mouth (Fig. 49). In some other species (N.

cathiae Inglis and N. sarcophili Cameron) the

buccal capsule is thinner, deeper, and some-

what domed, and the dorsal tooth ts erect and

pointed and does not seem ever to be pro-

truded through the oral opening. Moreover, in

N. tachyglossae and N. echidnae the tail of the

27)

female ends in a dorsal spine and two sub-

ventral processes, Jn species with a deeper

buccal capsule this type of tail has not been

seen.

It is concluded that species having these

characteristics in common should be grouped

in a genus for which the name Nicollinw is

availahle, For the other specics formerly in-

cluded in Nicollina a new genus, Woolleya, 1s

proposed.

Key to species of Nicollina

1. Worms more or less couled .... ..,

1. Worms not coiled a oe ae.

2. Dorsal ray with ihree pairs of branches

2, Dorsal ray with two pairs of branches ..

3. Buccal ring thick, lobed anteriorly . MV. ealabyi

3, Buccal ring not Johed, thinner and deeper _..,

N- inglisi

N. ritdei

NN, eamieront

bie Yr

4. Spicules bifid

4. Spicules simple

5, Spioules trifid —_ en

5. Spicules bifid. .., a eee 7

6, One lateral ala present N. echidnae

N, fachyglossae

N. mandeyi

N. havlist

6. Lateral alae absent .

7. Lateral alac present

7. Lateral alac absent

Nicollina echidnae Baylis

VIG, 50

Nicollina evhidnae (Baylis) Baylis, 1931,

Mawson, 1959; 154; syn. Nicollina echidnae

Baylis, 1930; 14. From Vachyglossus acu-

leatus.

The material examined in 1959 from an

echuina from Kangaroo L has now been com-

pared with the type material of the species, and

the identification confirmed. A transverse sec-

tion of the Kingaroo |. specimen is given. In

this species, and in N. tachyglossue, the excre-

tory pore, not mentioned by Baylis, is post-

oesophageal.

Nicollina cameroni Thomas, 1959; 154, from

the Echidna, Tachyglosvuy aenuleatys.

FIGS, 51-52

The paratype material of this species has

been re-examined. ‘Ihe body was described as

having two lateral alae and “some appearance

of fongiludinal banding’. Transverse sections

show a very slight widening of the cuticle later-

ally and in addition about 16 crests, most of

them lateral or ventral, The tooth is blunt, and

lies for the most part in the oesophageal fua-

nel.

This species. differs from others of the genus

in that the spicules are not divided distally, but

in view of the: similacity of other characters it

has been retained in the genus, ft differs very

markedly trom spectes of Austrostronevlus and

PATRICTA M. MAWSON

Prraustrostrongylus, in which the spicules. ace

single, in characters of the lateral alae, buccal

capsule, dorsal tooth, and bursa,

Nicollina haylisi n.sp.

FIGS. $3-59; TABLE 3

Host and locality; Tachyglossus aculeatus, Tas,

‘These are straight worms, with a cephalic

inflation, followed by numerous very low longi-

tudinal crests. Lateral alae ave absent. The

buccal capsule is very shallow, The oesophagus

is more of Jess cylindrical in its anterior two-

thirds then widens to an elongate bulb at the

posteriar end. The nerve ting surrounds it just

behind its midlength and the excretory pore

and cervical papillae are at about the same

level near its posterior end.

The lateral lobes of the bursa are very long

and are folded over each other, The externa-

dorsal ray arises from the dorsal and diverges

widely from it. The dorsal ray divides into two

bifid branches near tts distal end. The spicules

ure bifid for about half their length. The outer

branch of each ends in a barb and bears about

10 well-marked transverse ridges. in the middle

third of its length. ‘The eid of each branch is

surrounded by an ala, that on the smaller

branch much wider than that on the larger.

The gubernaculum is Stout, pitted on the sur-

face, and rather more than half the sprcule

in length.

The tail of the female is rounded and bears

a subterminal spike and two small lobes, The

vulva, a (transverse sli, ina depression of the

body wall, lics at a little less than a sixth of the

bodv length, or 20-27 tail lengths, from the

posterior end of the body, Uteri are opposed.

The eggs are 79-80 x 43-45 jam,

‘Vhe species is in many ways very like N.

tachyelossae, a straight worm with 8-10 longi-

tudinal crests and with somewhat similar, but

trifid, spicules. The two species difler however

in hody length, position of the vulva, and size

of the gubernaculum,

Nicollina munduyi nsp,

FIGS. 60-66; TABLE 3

Host and locality: Tarkyglossus aeuleatus and

Ornithorhynchus anatinus from Tas.

This is a short straight worm very simiur in

some respocts to N. echidnae. There are wo

jateral alae and about 20-22 longitudinal cuti-

cular crests, more or less: evenly distributed

around the body circumference for must of 1s

length, but. fewer towards the extremities.

The buccal capsule is short, ring-shaped; the

dorsal jooth is blunt and, at rest, hardly pro-

AMIDOSTOMATINAF FROM AUSTRALIAN MAMMALS 271

Figs. 48, 49.

Fig. 50.

Figs. 5t, 52.

Figs. 53-59,

Nicollitta tachyglossae, lateral and dorsal views of anterior end.

Nicollina echidnae, transverse section of body,

Nicollina camerani, Fig. 51.—Head. Fig, 52.—Transyerse section of body.

Nicollina baylisi. Fig. 53,—Oesophageal region. Fig. 54.—Lateral view of head. Fig,

55.—Trunsverse section of body just posterior to ocsophagus. Fig. 56—Posterior end

of male. Fig. 57.—Dorsal ray. Fig. 58,—One spicule. Fig. 59.—Tail of female.

Figs. 48, 49, and 57 to scale beside 51; Figs. 52 and 53 to same scale; Figs. 54, 57, 58, and 59 to scale

beside 59.

jects into the buccal cavity. The oesophagus is

cylindrical for most of its length, ending in a

bulb, The nerve ring lies at about half, and the

excretory pore and the small but distinct cervi-

cal papillae at three-quarters the length of the

oesophagus.

The end of the tail of the female bears a

terminal spike and two small subterminal lobes.

The vulva, at about 8-11 tail lengths in front

of the anus, lies between two rounded expan-

sions of the lateral alae. Eggs are about 75 x 40

wim,

The spicules are bifid, the outer branch of

each is longer and stouter than the other and

ends in a barbed point, the inner branch ending

simply. As only two male worms are present,

the spicules were not dissected out. Their

appearance is very similar to those of N. hay-

lis?, on which the terminal alae were not visible

until the spicules were out of the body. The

gubernaculum, at least two-thirds the length of

the spicules, is strongly built and its surface

pitted. The lateral Inbes of the bursa are not

particularly Jong. The rays are shown in Fig

63.

The species closely resembles N. baylivi, but

is distinguished by being distinctly shorter, with

lateral alae and with fewer and more promi-

nent cuticular crests, as well as by the shape of

the bursa, the absence of ridges on the spicules,

PATRICIA M. MAWSON

TABLE 3

Measurements of Nicollina baylisi, N. mundayi, N. calabyi, and N. inglisi. Unless otherwise indicated,

measurements are in jm.

Species N. baylist N. mundayi N. calabyi N. inglisi

Host echidna echidna platypus numbat numbat

Male:

Length (mm) 12,8-14.1 §.2,5.3 4.6—-5.7 2,4-3,.4 2.1-3.4

Oesophagus 500-525 445, 500 400-450 330-360 210-250

Ceph. inflation 80 (3x) 75,75 70-100 50-70 60-65

Antr. end—nerve ring 210-220 215, 220 220-230 120-170 100-120

—excr. pare 360-400 275, 315 370-390 160-260 1S0-180

Spicule 240-275 270, 295 250-270 600-700 400-440

Gubernacuwlum 145-165 140, 152 140-1660 80-110 70-80

Female:

Length (mm) 24.3, 25.3 6.5-8.1 7,7-8.0 2.5-4.2 2.3-3.4

Ocsophagus 600, 520 480-510 450-500 260-400 270-335

Ceph. inflation 100, 110 75-80 80-110 60-80 55-70

Antr. end—nerve ring 300, 270 210-240 230-240 120-20) 100-115

—excr. pore 500, 550 230-305 380-400 150-345 140-220

Tail 190, 150 120-140 140-165 70-130 60-90

Postr, end—vulva 3800, 4100 1250-1400 1500-1600 350-460 200-300

200,um

Figs. 60-66. Nicollina mundayi, Fig. 60.—Head. Fig. 6i—Oecsophageal region. Fig. 62.—Transverse

section of body. Fig. 63—Posterior end of male, ventral view. Figs. 64 and 65

and lateral views of region of vulva. Fig. 66.—Tail of female.

Figs. 61-66 to same scale; Figs. 64 and 65 to same scale.

Ventral

AMIDOSTOMATINAE TROM AUSTRALIAN MAMMALS

and the presence of culicular Maps beside the

vulva. The measurements ate similar to those

of N. evhidnae, bul the two species are dis-

tinguished by the shape and size of the spicules

and of the dorsal altd externo-dorsal rays, and

by the presence of the well-developed Icft

lateral ala in N. eehidnae.

Nicollina ealabyi n.sp.

FIGS, 67-72, TABLE 3

Host and locality! Myrmecobius fasciatus from

W. Aust,

The body forms a loose coil, The length of

the anterior cuticular inflation is about one and

a half times the hody width just behind the

inflation, and about 4 fifth to a sixth the length

of the oesophagus. The cuticle af the rest of

the body ts ratsed into 8-9 lateral and ventral

longitudinal crests, of which the lateral are thy

best-developed,

The mouth is surrounded by six small cuti-

cular lips. The buccal capsule is stourly built,

its anterior edge six-lobed, each lobe formed

by a thickening of the wall on the outer side

of the capsule. The dorsal tooth is rounded at

the apex, and reaches to about half the depth

of the buccal capsule. The cesophagus is wiser

in the second half of its length and is sur-

tounded by the nerve ring al the end of its first

quarter; the excretory pore hes at aboul the

ettd of the third quarter

The tail of the female is rounded at the tip,

with a subterminal spine af low ventral pro-

minence. The vulva is a transverse slit, three

to four (ail lengths in front of the anus, At the

evel of the vulva the cuticle is raised snto three

tongitudinal crests, one, bilobed, to the leét of

the vulva, a frilled narrow one to the right of

the vulva, and a longer wider one to the right

of this again (Fig, 72), The sizes and arrange-

mentot these crests gre similar in all the speci-

mons available The eggs are thin-shelled,

65-70 x 35-40 pm.

The spicules of the male are bifid for the

terminal 80-100 ym, the shorter of the two

ends pointed, the longer truncated and slightly

barbed, The gtbernaculum is elongate,

rounded at the ends, und thicker in the central

pacts. The bursa has a short dorsal lobe,

slightly separated From the large latero-ventral

lobes, The rays are arranged as shown in Fig.

69,

The species is placed in the genus Nicellina

because of the form of the huccal capsule and

tooth, It differs from the species frony mono-

tremes in the form of the dorsal ray, as well as

273

in the presence of 3 cuticular crests near the

vulva.

Nicollina inglisi i.sp.

FIGS, 74-76: TABLE 3

Host and locality: Myrmecohius fasciatus from

W, Aust.

This is a rather slender loosely coiled worm,

The length of the inflated cephalic cuticle is

about twice the width of the body just behind

it. There are 8-10 longitudinal crests on the

body, (wo dorsal and two Jateral, and the rest

ventral. The buccal cavity contains a large

blunt tooth. The oesophagus widens in its pas-

terior third and the nerve ring surrounds it al

about the end of the first. third, The excretory

pore is at the end of the second third.

The tail of the female lapers to & bi-lobed

tip, with a spike arising subterminally, The

vulva is a transverse slil siluated about three to

four times the tail length in front of the anus.

The cuticle just anterior und posterior to the

vulva is slightly inflated and strongly striated,

Amphidelphous, posterior uterus short, but

containing developing cgys. Eggs are up to 100

x 50 um,

In the male. one side of the bursa is slightly

longer than the other, but the rays are similarly

disposed. The dorsal lobe is short and the

dorsal ray thin (Fig. 74), The spicules are

bifid, with one branch ‘shorter than the other,

and the four tips, two from each spicule,

appear to be enclosed in one terminal ala

The species is close to N, calabyi, which was

found in the same collections. Tr is distin-

guished by the more slender build of the body,

the relatively longer cephalis inflation, the

slightly thinner-walled and deeper buccal cap-

swe, without anterior thickening; in addition,

the guhernaculum is longer, and there is a

small hut consistent difference in the dorsal

rays.

WOOLLEYA n.g.

Amidastomatinae: Small, more or tess coiled

worms with inflated cophalic cuticle and longi

tudinal cuticular crests behind this; huocal cap-

sule well developed, with pojnted dorsal tooth.

Male; bursa more or less symmetrical, dorsal

lobe small, dorsal ray dividing into two or three

branghes, externo-dorsal ray arising from

dorsal ray or separately: fateral and ventral

rays arising together, diverging from mid-

lengths; genital cane not strongly developed.

spicules single or divided at tips; gubernaculum

well developed. Female: tip of tail rounded

with thin spike, or tapering ta a point; vulva

274 PATRICIA M, MAWSON

304m

67 69

75 |il|

iy 71

Figs, 67-72. Nicollina calabyi. Fig. 67—Head. Fig. 68.—Transverse section of body, Fig. 69,—

Bursa. Fig. 70. -Gubernaculum and tips of one spicule, lateral view. Fig. 71.—Tips of

both spicules, ventral view. Fig. 72—Posterior end of female.

Figs. 73-76. Nicolfinw inglisi. Fig, 73,—Anterior end, Fig. 74—Bursa. lig. 75.—Tips of spicules.

Fig. 76.—Posterior end of female.

Figs 67, 70, 71, 73, and 75 to scale beside 73; Figs. 68, 69 and 74 to scale heside 69; Figs. 72 and 76

to scale beside 76.

towards posterior cnd of worm: mono- or di- W.. hickmant msp.; W. martini nsp., W.

delphous. Parasites of intestine of Australian monodelphis n,sp,

mammals, mainly of marsupials, The genus is named in recognition of the

Type species: W. sprenti n.sp. help given by Dr. Patricia Woollcy in collecting

Other species: W. cathiae (Inglis), syn. specimens from dasyurids.

Nicollina cathiae; W. sarcophili (Cameron), Woolleya species are distinguished from

syn. Nicollirta sarcophili; W- iota (Mawson), Nicollina spp. chiefly by (he shape of the buccal

syn Nicollina tota; W. acinucercus (Mawson), capsule which is cup-like with relatively thin

syn. Austrostrongylus acinocercus; W. walls, and by the shape of the sharply pointed

hydramyos (Thomas), syn. A. Aydronpyos; dorsal tooth, originating from the anterior end

AMIDOSTOMATINAK FROM AUSTRALIAN MAMMALS 134

of the oesophagus rather than, as in Nicollina

spp., from the anterior cnd of the wall of the

lumen of the oesophagus.

Figures are given of transverse sections of

W. acinocereus and W. hydromyes, which have

been re-examined but are not redescribed here

(Figs. 71, 78).

Key to specics of Woollceya

1. ‘Pail of female tapering to & point . 2

{. Tail of female rounded at tip, with spike . 4

2. Spicules not divided, or irifid! .

Ww. sareaphill

2, Spicules bifid .. 2 3

Female didelphaus WW, hydreinyiap

. Female meonodelphous WW. monodelphi

4. Spicules noi divided W. acinocerens

4. Spleules bifid... _)

5. Longitudinal create nore or "hex ‘evenly -distri-

buled around body

§. Longitudinal crests only on ventral surface. $

6, Tip of Jongcr branch of cach spleule en-

larged . |. W, jiora

6& Neither tip of spienles enlarged . theese

7. Dorsal ray ends in three pairs of branches

W. martiti

7. Dorsal ray ends in two pairs af branches

W hickmiani

8. Narrow lateral alae present W. cotkiae

8. Lateral alae absent —.. ... HW. sprenti

Woolleya sprenti n.sp-

FIGS, 79-85; TABLE 4

Host and localities: Desyuruy viverrinus from

Icena, Tas. (type host and locality); Arie-

chinus stuarti from Mt, Tidbinbilla, A,C.T,;

Dasyurops maculans from N.S.W., Thyla-

clings cynocephalas from Tas,

These are relatively long, slender worms,

some coiled louscly, some in a tight spiral; The

inflated cephalic cuticle, about a quarter the

length of the oesophagus, is lightly striated

transversely, the cuticle on the rest of the body

is more heavily striated and thrown into three

longitudinal crests extending most of the body

length on the ventral side.

The buccal capsule is large with a dorsal

tooth just over half the depth of the capsule.

Ventral teeth were not seen. The nerve ring

is. just behind the mid-oesophagus and the ex-

crelory pore near the posterior end of the oeso-

phagus.

The posterior end of the female narrows

abruptly just in front of the anus and the tail

is digitiform with a rounded tip bearing a ter-

minal spike. The vulva is about five to eighr

tail-leneths in front of the ants. Two ovejectors

aud Wteri are present, the posterior much the

shorter,

The bursa is symmetrical, its dorsal lobe

short but quite distinct. The arrangement of

the bursal rays is shown in Figs. 82 and 83.

Each spicule hifurcates at abouf a fifth its

length; one branch is slightly longer and stouter

than the other, and is curved inwards at the

tip. The gubernaculuin is long and wide, the

central part more heavily chitinised,

The specimens (two females) from Thyla-

cinus cynocephalus agree in all particulars with

the types. In view of the different host, it is

possible that they may belong to a different

species, distinguishable only by characters of

the male, As the host species is now virtually

extinet it is unlikely that a male will be found,

unless in some museum. The specimens des

cribed here were found in a museum specimen

of the host, through the enterprise of Professor

J.. F. A. Sprent,

This species mast closely resembles WN.

Aydrontyos Thomas in the shape of the spi-

cules and the arrangement of the dorsal ray-

The two species differ however in the lengths

of spicules and guhernaculum and in the shape

of the femate tail.

Woolleya martini nsp,

FIGS. 86-89; TABLE 4

Host and localily; <Antechinomys

from Sandringham, Qld.

This is a relatively small species, with 10

longitudinal cuticular crests. The cephalic in-

flation of the cuticle is aboul twice as long as

tts diameter, and between a third and # quarter

the length of the oesophagus. ‘The cuticle

around the mouth forms six distinct lips, The

dorsal tooth is about half the length of the

buveal capsule. The exerectory pare lics iat or

just behind the base of the oesophagus,

The spicules are bifid in their distal quarter:

both branches are slender, one a little more

curved and slightly longer than the other. The

arrangement of the bursal rays is shown in

Fig. 88.

The body of the female narrows just in front

of the anus and ends in a digitiform tail,

rounded at the tip and bearing a terminal spine.

Only two, sub-veutral, crests continue posterior

to the vulva.

This species js distinguished from W/, sprenr

chiefly by the number of cuticular crests, and

by the origin and shape of the oxterno-dorsal

Tay.

spencert

1Tke number of terminations of exch spicule is net stated dn the description of this species.

PATRICIA M. MAWSON

276

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y ATEaVL

AMIDOSTOMATINAE FROM AUSTRALIAN MAMMALS

504m

50m

Fig. 77. Woalleya hydromyos, transverse séction of body.

Fig. 78, Woolleya acinocercus, transverse section of body.

Figs. 79-85.

Woolleya sprenti, Fig. 79.—Anterior end, Fig, 80.—Oesophageal region. Fig, 81.—Trans-

verse section of body. Fig. 82.—Posterior end of male, Fig. 83,—Dorsal and one extertio-

dorsal rays. Fig. 84.—Spicules. Fig. §5.—Posterior end of female.

Figs. 77, 79, and 83 to scale beside 77; Figs. 78 and 84 to scale beside 84; Figs, 81 and &2 to Scale

beside 82.

Woolleya bickmani n.sp.

FIGS. 90-93; TABLE 4

Host and locality: Antechinus stuartii from

Condor Creek and Mt, Tidbinbilla, A,C,T,

These are fongish coiled worms. The cuticle

is raised into ten or twelve longitudinal crests,

extending for most of the body length, and

more or less evenly distributed around the

body, the widest gap being on the dorsal side

(Fig. 91). The buccal capsule is shallow and

the dorsal tooth short.

The bursa is more or less symmetrical, the

dorsal lobe not separated from laterals. The

arrangement of the rays is shown in Fig. 92,

The spicules bifureate at about 3/4 or 4/5

their length; each branch ends in a blunt point,

PATRICIA M, MAWSON

Wooalleya martini. Fig. 86.—Anterior end. Fig, 87.—Transverse section of body. Fig.

88.—Part of bursa. Fig. 89.—Posterior end of female,

Woolleya Aickmani. Fig. 90—Antetior end, Fig. 91—Transverse section of body hebind

oesophagus. Fig. 92,—Bursa. Fig. 93.—Posterior cnd of female.

Woolleya monodelphis. Fig. 94.—Anterior end, Fig. 95,—Transverse section of body.

Fig, 96.—Bursa, Fig. 97.—Spicules. Fig. 98—Posterior end of female.

Figs. 86, 91, 94, and 97 to scale beside 94; Figs. 87, 88. 90, 92, 96, and 98 to scale beside 88.

the longer one rather more curved at the tip.

A thin plate-like gubernaculum is present.

The posterior end of the body of the female

is slightly swollen; the tail tapers somewhat and

is rounded at the end, with a terminal spike.

Two ovejectors are well-developed. Eggs are

about 60 x 30 ym.

This species differs from W. martini in the

distribution of the cuticular crests and in the

branching of the dorsal ray (see Figs. 88, 92).

Woolleyi moenodelphis nsp.

FIGS. 94-98: TABLE 4

Host and locality: Antechinus stuartji from

Condor Creek, A:C.T.

This is a very small specics; the anterior end

of the body ends in a more or less tight. spiral:

the posterior is curved, and in the Female dis-

tinctly swollen in the region of the vulya. There

are four longitudinal ventral crests, on the an-

terior two-thirds or more of the body. The

AMIDOSTOMATINAE FROM AUSTRALIAN MAMMALS

cephalic inflation is about two-thirds the length

of the ocsophagus. The buccal capsule is large,

the dorsal tooth very small. The posterior end

o! the oesophagus was secn clearly in only one

specimen, and the nerve rig and exerttory

pore were not secn im any,

The arrangement of the bursal rays is shown

in Fig. 96. ‘The dorsal pay is unusually stout,

and arises separately. The branches of the

dorsal ray are very small, and it is possible that

the final branch shown in Fig. 96 is divided.

The spicules ate hifid for ahout one third of

their Jength. one branch of each being thicker

and slightly longer than the other. A slender

gubernaculum is present.

Fhe tail of the female is relatively Jong and

tapers to a fine point The vulva lies about one

tail length in front of the anus, between two

short and wide sub-ventral crests or flaps,

There is only one ovejector and uterus, the

antenor. No eggs were seen,

This species differs from all others referred

to Woolleya in being monodelphous, in the

wide externo-dorsal rays, and in the very small

279

size, and from most of the species in the shape

of the tail of the female.

Acknowledgements

The collections used in this sludy were made

available by a number of people, Some material

from Tasmania was sent by Dr. B. Munday

and Mr. R. Green of Launceston, and some

by Or. John Hickman of Hobart. Dr. John

Calaby (C.S.LR.0. Division of Wildlife Man-

agement) sent some nematodes from a numbat;

Dr. P. Woolley contributed most of the mate-

rial from Anfechinus stuartii. "The bodies of

Antechinomys sp,, native cats, and a numbat

were donated by my colleague, Professor P_ G,

Martin. Material from Queensland wallabies

was sent by the late Dr. M, J. Mavkerras, Pro-

fessor Sprent (Dept. of Parasitology, Univer-

sity of Queensland) very kindly let me have

the two Worms from the thylacine,

All of these people have taken considerable

trouble to send worms. or host bodies in a good

state of preservation, and [ am very grateful

to them.

Most of the work was carried out while in

receipt of a Rural Credits Research Grant,

References

Bayus, H. A. (1930) —Four new: trichostrongylid

nematodes from Queensland. Ann. Mag. nat.

Hist, 1 (6), 1-18,

Bavots. A, A. (1931)—A nomenclatural correc-

tion, Aan, Mag, nat, Hist, 10 (7), 550,

Camenon, 'T. W. M. (1931).—On a species of

trichostrongyle from the Tasmanian Devil. 7,

Helminth. 9, 153-156,

Cuanpior, A. C, (1924) —A new genus of tricha-

slrongylid worms from the kangaroo. Pera-

sitology 16, 160-163.

Durette-Desset, M. (1964),—Les systémes

Warétes cuticulaires chez les nématodes hélig-

mosomes, Etude de cing espéecs parasites do

rongeurs de la Maboké. Cahiers de La

Mahoké 2, 40-78.

Digerre-DesseT, M. (1966)—Sur deux nou-

yeaux trichostrongyles purayites du Porc-Epic

au Viet-Nam. dArnntls. Parasit. hum. comp. al,

453-466.

Ineuis, W. G. (1968).---The geographical and

evolutionary relationships of Australian tri-

chostrongyloid parasites and their hosts. J.

Linn, Sac, 47, 327-347.

Jonnston, T. H., & Mawson, P.M, (1938).—

Some nematodes from Australian marsupials.

Ree. S. Aust. Mus. 6, 187-198.

Ionwston, T. H., & Mawson, P. M. (1939).—

Stronyylate nematodes from marsupials in

New South Wales. Prec. Linn. Sac. NSW.

64, 513-536.

Toumsron, T.. H., & Mawson, P.M, (194038) —

Nematodes from South Australia. Trans. R,

Soc. S. Aust. 64, 95-100,

Jounston, T. H., & Mawson, P. M. (1940b).—

New and known nematodes from Australian

tea Proc. Linn, Soc, NSW. 65, 468-

476,

Jounsion, T. H., & Mawson, PL M, (1949).—

Some nematodes from Australian hosts to-

fether with a note on Riahditis allgeni. Trans,

R. Sov. §. Aust. 7a, 63-71.

Mawson, P, M. (1960),—Nematodes belonging to

the Trichostrongylidae, Subuluridae, Rhab-

dinsidae, and Trichuridac from bandicuats-

Aust. J. Zool. 8, 261-284.

Mawson, P. M. (1961). —Trichostrongyles from

rodents in Queensland, with comments on the

genus Longistriata (Nematoda: Heligmoso-

matidae). Aust. J. Zoal. 9, 791-826,

THomas {—Mawson), P. M, (1959).—Some

nematode purasites from Australian hasts,

Trans. &, Sov, S. Aust, 82, 151-162.

THE STRUCTURAL GEOLOGY OF THE WARREN NATIONAL PARK

AND THE WESTERN PORTION OF THE MOUNT CRAWFORD

STATE FOREST, SOUTH AUSTRALIA

BY K, J. MILLs*

Summary

MILLS, K. J. (1973) -The Structural Geology of the Warren National Park and the Western Portion

of the Mount Crawford State Forest, South Australia. Trans. R. Soc. S. Aust. 97(4), 28 1-3 15, 30

November, 1973.

A structural study of coarse-grained sillimanite-bearing mica schists and gneisses exposed on the

southern shores of the Warren Reservoir, south-cast of Williamstown, has revealed evidence for

three successive phases of strong compressive deformation, each characterised by the introduction

of new structural elements. These rocks stratigraphically overlie a thick crossbedded schistose

metasandstone unit which closely resembles the Aldgate Sandstone of the Adelaide Supergroup.

This metasandstone unit also displays evidence for three superimposed fold episodes. Coarse

grained sillimanite-bearing mica schists and gneisses underlying the metasandstone have a similar

lithological and compositional range to those above the metasandstone, but are more complexly

deformed and show indications of earlier compressive deformation events. Careful mapping of the

contact between these older schists and the metasandstone has revealed an angular unconformity in

several localities, thus re-establishing an exposure of pre-Adelaidean basement, herein named the

Warren Inlier. Rocks within the inlier have been reconstituted at high temperatures along with the

Adelaidean sequence and have structural characteristics quite unlike those of the previously

described basement inliers within the lower temperature metamorphic environments of the Mount

Lofty Ranges. Detailed mapping has established that a period of major thrust moyements took

effect during and after the second compressive deformation in the Adelaidean sequence, and that

these thrusts were later folded during the third compressive deformation. The final significant

tectonic event is recorded by the Williamstown-Meadows Fault, which brought the amphibolite

facies schists and gneisses into conjunction with biotite zone phyllites.

The fortunate combination of thrusting and updoming in subsequent folding, with later uplift on the

Williamstown-Meadows Fault in this part of the central Mount Lofty Ranges, has enabled erosion

to unveil a tectonic window, herein named the Williamstown Window, through which may be read

the structural history of the lowermost tectonic and stratigraphic leyels of the Upper Proterozoic

sedimentary pile and the underlying basement gneisses.

THE STRUCTURAL GEQLOGY OF THE WARREN NATIONAL PARK

AND THE WESTERN PORTION OF THE MOUNT CRAWFORD STATE FOREST,

SOUTH AUSTRALIA

by K. J. Mitis*

Summary

Miuus, K. .|, (1973).—The Structural Geology of the Warren National Park and the Western

Portion of the Mount Crawford State Forest, South Australia, Trans, R. Soc, 8, Ausé.

97(4), 281-315, 30 November, 1973.

A structural study of coarse-grained sillimanite-bearing mica schists and gneisses exposed

an the southern shores of the Warren Reservoir, south-east of Williamstown, has ‘evenled

evidence for three successive pluses of strong comipressive deformation, each characterised by

The introduction of new structural elements. These rocks stratigraphically overlie a thick cross~

hedded schistose tmetasandstone unit which closely resembles the Aldgate Sandstone of the

Adelaide Supergroup, This metasandstone unit also displays evidence for three superimposed

fold episodes. Coatse-grained sillimanite-bearing mica schists and gneisses underlying the meta-

sandstone have a similar lithologica] and compositional range to those above the mctasandstone,

but are more complexly deformed and show indications of earlier compressive deformation

events. Careful mapping of the contact between these older schists and the metasandstone has

revealed an angular unconformity in several localities, thus re-establishing an exposure of

pre-Adeélaidean basement, hetein named the Watten Inliet. Rocks within the inlier have been

reconstituted at. high temperatures along with the Adelsidean sequence und have structural

characteristics quite unlike those of the previously described basement inliers within the lower

temperature metamorphic environments of the Mount Lofty Ranges. Detailed mapping hus

established that 4 period of major thrust movements took effect during and after the second

compressive deformation in the Adelaidean sequence, and that these thrusts were later folded

during the third compressive deformation, ‘The final significant tectonic event is recorded

by the Williarmstuwo-Meadows Fault which brought the amphibolite facies schists and gneisses

into conjunction with biotite zone phyllites,

The fortunate combination of thrusting and updoming in subsequent folding, with later

uplift on the Williantstown-Meadows Fault in this part of the central Mount Lofty Ranges,

has enabled erosion ta unveil a tecfonic window, herein named the Williamstown Window,

through which may he read the structural history of the lowermost tectonic und stratigraphic

levels of the Upper Proterozoic sedimentary pile and the imderlying basement gneisses,

the highest peak in the area and from its

central location one can view the rugged

Introduction

This paper is concerned with the elucidation

of the structural history of a key area of

approximately 40 km? in the central Mount

Lofiy Ranges. The atea is located south-east

of Williamstown and extends south and west

of the Warren Reservoir. Much of the area is

virgin scrubland, parts of which have been

recently acquired by the National Parks Com-

mission (Warren and Hale National Parks), or

are wnder the control of the Engineering and

Water Supply Department. or form perl of

the Mount Crawford State Forest. There are

a few small grazing properties in Dead Horse

Gully (Watts Gully) and south of the reser-

vair. Lookout Tower Hill (over 525 m) forms

guilied scarp country of the Warren National

Park falling off to the west, and the gorge

of the South Para River and the Warren Re-

servoily to the north. Outcrops are frequent

and fresh on these youthfully eroded slopes,

To the south-east and south a much more

mature topography, containing remnants of

laterised erosion surfaces, exhibits only scat-

tered bedrock exposures, most of which are

deeply weathered.

The area was the scene of a goldrush in

TRRS, and this. led lo the appearance of one

of the earliest geological maps to be published

in this state (Brown & Woodward 1886). In

* Deparimicat of Geology ang Geophysics, The University of Sydney, Sydney, N.S.W. 2006.

482

describing the bedrock around Watts Gully

(See Fig. J) Brown & Woodward clearly

recopnised (wo mictamorphice sequehecs—

micaceous and chloritic and clay slates with

beds of quartzite und schistose sandstunes; and

highly metamorphosed rocks consisting of mica

schist, quiartzites, sandstones and ynvisste

rocks. The goldficlds were situated in the

highly metamorphosed sequence.

Howchin (1906, pp. 254-256), referring to

the ridge between Williamstown and the Suuth

Para River. recognised and described the

“basal grits” of the “Adelaide Series", although

here they have been strongly metamonphised

and intruded by pegmatites. An older base-

ment of highly foliated mica schists, pene-

irated with pegmatites, was observed to

underlie the basal grits in the goree of the

South Para River, and to be separated from

them by a Brass covered, but nevertheless

“abrupt and strongly defined” junction.

Howchin (1926) presented the resulis of

more extensive obsetvationy in this area, in-

cluding a [3 km section extending ENE from

the “Houghtonian” schists in the South Pita

gorec oear the Warren Reservoir Weir,

ihrough the basal grits inte a sequence of

rocks, comprising the Barossa Ranges, which

he eqvated with the lower portion of the

“Adelaide Series". Although clearly recog-

nising the existence of an older basement in

this area, Howchin included within his tasye-

ment some coarsely crystalline schists, such as

Brown & Woodward's highly metamorphosed

Tucks of the Gumeracha Goldficlds, and the

host jocks of the rutile deposits near the

reservoir, which are now known to oaverbie the

“basal grits’.

Hossfeld (1935) refuted many of Howchin's

Views and, although accepting the “basal

grits” south of Williamstown, regarded the

rocks gist al Williamstown os an older

sequence {Woolnough’s Barossian) which

underlay the grits. Miles. (1950) published a

map incerporating the north-western part of

the arca under present consideration and

showed that highly metumearphosed Adelaide

System rocks overlay the haematitic schistose

sandstones, and were faulted against low grnde

Adelaide System rocks belonging to a much

higher stratigraphic level.

Alderman (1942) regarded the high-grade

aluminous schisis and gneisses, and their con-

tained sillimanite, kyanite and clay depostis,

north of the reservoir as products of an exten-

sive metasomatic alteration of original country

kK. 3, MILLS

rocks of regional biotite grade This concep!

of extensive metasomatic activity in the areca

was further adyanced by Campana (1953) and

Campana ef «wl. (1953) in the interpretation oF

the Gawler Geological Sheet. Schists which

Howchin saw as an underlying basement to

the basal grits were interpreted by Campana

as a metasomatic facies of the busal beds.

Hence these rocks were shown as the “Alu-

minous metasomatic zone of South Warren

Reservoir” on the Gawler Geological Sheet.

Campana accepted Howchin's view that the

sequence cas! of this zone could be correlated

with rocks ef the Adeluide System.

Previously (Mills 1963), | authited the pet-

tology of the yarious rock units in the area

south of the Warren Reservoir and considered

that the schists were the products of normal

amphibolite facies metamorphism of rocks of

appropriate composition, doubting the need

for extensive metasomatic activity. The schists

and gneisses south-west of the reservoir were

Observed to underlie Howchin’s “basal grits”,

but at that stage a convincing unconformity

had not been identified. "Whe schistose meta.

sandstone unit became more micactous

towards its base and was thought to pass

conformably downwards info micueeuus

schists and gnetsses.

Whilst studying the mesoscope geometry ol

structures in these high-grade schisis in the

summer of 1967, L discovered that schisis

below the metasandstone unit were much

more complexly deformed than those above,

despite similwritics in lithological character,

and this Jed tu the distuvery of several out-

crops displaying a distinct stratigraphic uncon-

formity between the metasandstone and the

underlying schists, in a section which has

beeome the southern portion of the Warren

National Park, Through personal conmmuni-

cation with Messrs. Ofller and Fleming. this

tediscovered bascment inlier appeared in their

published synthesis of the structural and meta-

morphic. history of the Mount Lofty Ranges

(OMer & Fleming 1968, pp, 248, 252), Since

that time I have engaged in several summer

fleld excursions to the wrea, mappiny in further

detail, and the following account presents the

results.

The area has been mupped using werial

photographs and a base map constructed from

an uncontrolled mozaic, Theré may, therefore,

be slight dislorlions from true orthographic

projection in parts of the mip, bur it has

been found that the grid used on the Adelaide

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

und Gawler 1:63,360 Military Sheets may be

satisfactorily imposed. Ft is importint 1

realise Thal the maps, as reproduced here.

present interpreted boundaries and fuults.

Reasons governing these interpretations will

be outlined below, The reader may be dis-

appointed to discover, particularly in the

south-eastern poriton of the areca, that lines

on the map may seem ta have no readily

apparent meaning in the fieki. They are, how-

ever, based on the close inspection and inter-

pretation and careful plotting of al) available

field exposures over the whole area covered

by the map.

Stratigraphic and Metamorphic Retationships

Between Mapped Lithological Units

PRELIMINARY COMMEN1S

The presence of an older Precambrian base-

ment inlier, here referred to as the Warren

Thlier, has now been flimly established an the

hasis of observed wnconformuble relationships

and on structural grounds. Overlying this base-

ment is a mantle of Adejaidean sediments,

beginning with a thick schistose metasandstone

of Aldgate Sandstone type. and passing

upwards into a varied sequence of pelitic,

arenaccous and calcareous beds. The Ade-

laidean =omuantle has suffered three strong

compressive deformations and course recrys-

tallisution in amphibolite Facies metamorphism.

Strong thrusting from the east accompanied

or followed the second deformation and

resulted in several strike Faults with extensive

aggregate movement. The largest of these

faulis hus brought a kyanile-andalusite [acies

sequence of siniple structural chyracter into

conjunction with a cemplexly deformed silli-

manife-muscovile facies sequence, The thrust

slices were folded in a third deformation,

which also updomed the hasement inlier. Fol-

lowing this deformation, the whole area was

uplifted by a very large displacement on the

Williamstown-Mesdows Fault, bringing amphi-

belite facies tocks into conjunction with a

biotite grade sequence, marking the western

boundary of the area. Figure | shows the

subdivision and distribution of lithologicul

units,

THE BASEMENT (Warren INvter)

The pre-Adelaidean basement schists and

gneisses are exposed over an area of approxi-

mate 6.5 km*, These rocks clearly underlie

the cross-hedded schistose metasandstone of

the Adelaidean sequence and are separated

283

[rom that metusandstone unit by an angular

ungonformity, It is proposed that the mame

Warten Inlier be apphed to this basement ex-

posure. The South Para River, downstream

from the Warren Reservoir, has cul a rugged

gorge through this inlier, and the spillway of

the reservoir, like thal of the South Paria

Reservoir further downstream, has been con-

structed on the older Precambrian basement,

There are also Jarge exposures of the basemetit

racks north and south of the South Para

Borge, and in particular at the southern end

of the Warren National Park.

The fresh anificial exposures on the over-

flow race at the southern end of the Warren

Weir provide a conveniently accessible loci-

tion for examining the general nature and

structugal complexity of these rocks. The pre-

dominant rock here is a coarse-grained schis-

lose quartz-felspat-mica gneiss with prominent

lenticular quartzofelspathic und micaceous

compositional layers developed on all visible

scales and displaying various mtnecate fold

structures. A typical specimen is composed of

60% plagioclase (An 14) as unzoned rarely

twinned 0,5-1 mm granoblasts; 10% quartz;

20% biotite as plates up to 3 mm in diameter,

interleaved with some muscovite and altering

to. chlorite; 10% fibrolitic sillimanite, which

has undergone almost complete: sericitisation

and recrystallisation to new decussate muscn-

vite flakes, distributed in lenticular layers; and

the minor accessories rutile, zircon and apatite.

The coarse crystals in this rock are observes

to be mimetic after crenulations in the gneis-

sosity, although there are also pronounced

late strain features, such as bent mica flukes

and deformation lamellae and strain bands tn

ajuartz. The size of the quartz inclusuins its

the plagioclase grains and of accessory zircons

indicate u likely pelitic parentage, There are

rare layers of very coarse biotite rich schist,

and one of these grades into a biotite antphir

holite with accessory rutile, This rock is

composed of about 80% of poorly oriented

interlocking hornblende poikiloblasts 1-2 mm

in diameter, containing about 5% of small

quartz, biotite, epidote, carbonate and opaque

inclusions. The amphibole is pleochroic from

pale lemon to blue-green and is characterised

by strong ratilé exsolution, Thick bioiite flakes

(5%) altering to chlorite are scattered through-

out. The leucocratic fraction fs composed of

equal amounts of quartz and plagioclase (An

45-50) eranoblasts. Rutile, apatite, epidore and

opaque prains are accessories. The textures

Hac

amt 4 PAW

|= —

w”

sew

aj Greys SENS SP

3] F52]y | pte

stewie ¢! oe

> Fy

a Pe] Bilt Kho

Stu a ESI Sor ea ’

Bie = o msl | ;

mje E

uw = o l<

Ola zz _

al’ 2 es ae

2h 5

Tr wads =.

a ee >

a as >

= pO A

Ener

Loe

Roe ~

Ste

pee

Nee

NATIONAL -"»

yg SEE

WOES fo oa

<3.

owe

mh ee

Fiz 1

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

LEGEND FOR

LITHOLOGICAL MAP

im =| Alluvium

( Brotite Zone Rocns.

| Fine-qramed phyllites. dolomites,

dolamihc phyllites, quartzites

HvaNrte-ANDaLusITe ZONE Rocks

Calc-silicate rocks (diopside, scapalita,

amphibole), fine grained khrotted schist

Fine-qrained Knotted schist, pyritie

schist, quartzose schis!

Pink felspathic quartzite horizon

Tramotite rack with interbedded

felspathic and actinolitic sandstone

]

f acy Felspathic sandstone

Siitimanite-Muscovite Zone Rocks

Granite qnaiss (quartz-microcline-

Plagicclase-bictite-muscovite gneisal

Course-grained crumpled schist

(kyanite; slaurolite, sillimanite)

Tremolita rack horizon

Felspathic sandstone with Fitanifercus

haematite and muscavite

” BASEMENT

Coarsé-qrained crumpled schist and

Bad gneiss \siflimanife-muscovite zone}

Tertiary deposils and minor intrusions nat -shown

ee Inferred Fault

—— Inferred Thrust

en Fault Mélange

1 Le Lenin ty

’ Se

Felice J — Road or Tack

~ River or Watercourse

* Mine or Prospect

Gid Adapted From 1000yd. Military Grid System

Fig. lL. (Opposite). Lithological map showing the

distribution of the principul divisions of

rock types in the region around rhe Warren

Reservoir.

285

and the composition of this rock suggest an

orginal marl. Pods and lenses of quartz and

segregation pegmatites are also common in

the outcrop.

No attempt has been made 16 map litho-

logical variations across the remainder of the

inlier. although exposure is sulliciently good

for this ta be a promising line of attack.

Reconnaissance observations have not revealed

a great deal of lithological variation. Almost

all rocks appear to have had a pelitic or

psammiopelitic ancestry, although there are

some more quartzofelspathic varieties in the

South Para downstream from the weir. The

biotite-rich schists and amphibolites noted a1

the weir are to be found elsewhere as small!

isolated. occurrences, but are apparently quite

sparse. No rocks of the “Houghton diorite”

type (Benson 1909) have been found in this

inlier. The only rocks with an intrusive charac-

ter are scattered quartz pods and dykes and

abundant pegmatoidul rocks, mostly ot a

segregation type but with rarer crosscutting

varieties containing sparse beryl and tourmu-

line.

Amongst the pelitic and psammopelitic

meisses compositional variations range from

sillimanite (sericite)-rich gneisses (e.g. grid

rets. 909082 and 916106), through varieties

with less sillimanite, similar to the weir

gneisses described above, to quartzofelspathic

encisses lacking sillimanite. Some of the latter

may contain abundant well-twinned microcline,

Or puss mto rocks consisting almost entirely of

muscovite und quartz, such as the coarse-

grained crenulated schist immediately under-

lying the melasandsione on the shore of the

reservoir north of the weir. Within each com-

positional group are a number of structural

variants, such as folded, crenulated, lineated,

banded, striped or granulose gneisses, depend-

ing oo the Jocal structural history of each

rock.

A study of the metamorphic minerals and

textures of the basement rocks has indicated

that they were brought to a metamorphic

temperature peak Jate in their structural his-

tory. This metamorphic peak was apparently

uniform over the whole inler and reached

the stage where sillimanite was stable in the

presence of muscovite in aluminous. schists,

No evidence has been found for any extensive

breakdown of muscovite and potash felspar

(mictocline) is confined to the non-aluminous

varieties. Of other index minerals, garnet and

kyanite have been rarely recognised and anda-

236

lutsite aiid staurolite have not so far been

identified, It seems that (he basement rocks

have an apparently similar metamorphic his-

tory to the Adelaidean schists and vneisses

Immediately overlying the metasandstone unit,

and it is helieved that the metamorphic peak

indicated in the basement rocks was identical

to that which may be deduced from tocks of

the Adeluidean mantle. It seems clear that the

pre-Adelaidean metamorphism of the base-

ment rocks involved lower grade conditions

thai those reached in the early Palaeozoic

urageny which affected both basement and

mantle.

Spry (1951) reported a fall in grade from

south to north, involving sillimanite, garnet

and biotic zones, for the early pre-Ade¢laidean

metmorphism of the nearby Houghton Inlier,

which could be construed to fit the above

conelusion, bul Talbot (1962)! has disputed

this grade variation. Talbot (1963) has shown

Ihat the Houghton Inlier has suffered three

metamorphisins. ‘I'wo pre-Adelaidean episodes,

the earlier involving upper amphibolite facies

conditions, and the tater involving pervasive

greenschist facies retrogression accompanying

strong phyllonitisation, were averprinied by a

ereenschist facies (biotite zone! episode accom-

panying the Palacozoie metamorphism of the

Adelaideun mantle. A tentative Rb-Sr date of

867-4492 my, has been suggested for the

upper amphibolite facies. metamorphism

(Couper & Compston 1971), while the Palaeo-

Zoic metamorphism has heen daled al 490415

m.y. (White, Compston & Kiceman 1967).

Jn the Warren Inlier the Palaeozoic meta-

morphism has obscured all evidence of pre-

Audelaidean metamorphic grade in the base-

ment cocks. [| is conceivable that rocks of

the Warren Inlicr have passed through « phyl-

fonilic stage similar to the Houghton Inlier,

bul there & so far no cvidence of at or of any

earlier hivher grade metamorphic episodes,

Che late metamorphic hiktery of the

Warren Inljicr tocks and the overlving Ade

laidewn schists is also similar, involving per-

yasive retrogression of sillimanite to sericite

and muscovite and uf biotite to chlorite, and

she appearance of late strain features such as

hent and kinked micas, lamellar twinning in

plagieclase and deformation bands and lamel-

la@ an quartz.

K. J. MILLS

THE LINCONFORMITY

The actual surface of unconformily is only

clewly exposed in two loeulities; on private

Jand south of the reservoir (grid ref, 925108),

and in the southern part of the Warren

Nuwtional Park (grid refs, 909088-91 2090). The

Warren National Park exposures ate the must

instructive and will be described first.

Several large exposures in the southern

portion of the Warren National Park display

a fingernail sharp unconformity surface, There

is a large angular discordance between the

gently south dipping quartzofelspathic banding

in the basement gneisses and the near vertical

hedding of the overlying metasatidstone

(Fig. 3f). The basement gneisses; here ure

coarse-grained, mica-tich and schistose. The

preminent quartzofelspathi¢ bands may be

related to original bedding, but are probably

transposed and Iack stratigraphic significance.

The basal units of the overlying metasandsione

ure nich in muscovite and strongly schisiose.

These unils become quite friable on weather-

ing, resulting in a ntgative relief against the

more massive basement gneisses, A basal con-

vlomerate is develuped locally at grid ret.

911088. The pebbles range up ro 30 cor in

length, aré moderately angular and are locally

derived from the quartzofelspathic bands of

the underlying basement. The bed is up to

half a nietre thick and i observed to he

welded onto the basement. In adjacent out-

crops the conglomerate is absent and # musco-

vite-vich schistose metasandstonc. characterised

by an unusual abundance of haematite ind ou

few scattered rounded quartz of quartzite

pebbies. to a few centimetres in diameter, is

welded directly on to the basement with a

sharply defined contact. A strong metamorphic

and situctural convergence of the basement

and the overlying Adelaidcan beds has ob-

scured ihis camlact in some exposures. Where

the contact is clear the unconformity surface

is seen to he quite irregular in detail, with

harder bands in the basement protruding into

the basal beds. A metre or so above the

unconformity the bedding in the metasaned-

alone is unallected by these irregularitics.

Following the inlier boundary to the sauth-

west from the above localities, no actual

exposiires of the unconformity were seen,

although a boundary between the basement

! Talbot SLL. (1962)—A study of the structural and metamorphic relationships between older and

younger Precambrian rocks in the Mr. Lofty Rauge Olary Are; South Australia, Univ, Adelaide,

Ph.D, Thesis.

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

encisses and the metasandslone can be

mapped, the basal metasanudstone exposures

being agam enriched jn hacmatilc, In the

south-west corner Of the inher the boundary

begins to turn castwards aod disappears

beneath alluvium. Apart from one smul! ex-

posure of cross-bedded hucmatite-rich micta-

sandstone overlying the basement a little

further castwards, no other exposures of the

contact are seen, the southern ind eastern

sides of the inlicr being delincuted by a major

thrust fault.

Following the inlier boundary to the north-

enst from the Warren National Park expo-

Sures, the basal metasandstane beds are

haematite and muscovite-rich, but no actual

unconformity surface was observed. ‘lhe actual

contact lies near the base of a sleep escarp-

ment of husement gneisses. This escarpment

is related to the friability of the basal beds of

the Adeluidean sequence and the erosional

Teststance of the basement gneisses. Rainfall

tun-off trom the basement genciss exposures

engenders a thick undergrowth near the

comlact,

On a track extending porth-west of Lookout

Tower Hill (grid ref. 918105) a haematite-rich

quartz-museayvite rock is seen close to the

inlier contact as Ihe lowest bed in the meta-

sindstone sequence. This rock is composed

of 65% quartz as large grattoblasis to 3 mim,

25% muscovite, 10% haematite, and 5%

barite. as evenly distributed interstitial grains.

Much post-crystalline sttuin ts evident in the

quartz and muscovite.

Following the inlier boundary westwards

around several folds, no actual exposures of

the unconformity surface were found. The

basal beds of the Adelaidean are muscovite-

rich metasandstones, usually bearing notable

hucmalile or a trace of biotite, Bedding is out-

lined by yuartz-rich bunds, und occasional

Tounded quartz or quartzite pebbles to 3 cm

in diameter are scattered along some bedding

planes, The adjacent bastment is mostly a

inieu-rich schist, No unconformity surface was

observed along the long meridjanal western

contact of the inher although the boundary

can be closely mapped. Again muscovite-rich

schistose metasindstones are churactenstic al

ihe basal beds, On the Engineering and Water

Supply access road (grid tef. 902125) a two

metre gap of soil and prass separates whit

appears lo be the basal bed, a coarse hacma-

lite-rich quartz-muscovite metasandstone with

& few small pebbles, from strongly folded

287

coarse-grained quarlz-lelspar-bidtile-muscayile

gneisses of ibe basement. Th haematite-ch

bed can be seen at several points further nor h

hear the inlier contact, but nearer the porthem

tip ef the inter this basal bed has apparently

lensed out and beds of muscovite-rich meta-

sandstone [rom slightly higher in the sequence

come to rest on the basement. From the

northern tip of the inticr (Hale National Park)

to the reservoir the inlier contact was nat

eusily mapped. The unconformity exposure

described by Hossteld (1935, p. 37) could not

be found, although bath busement and meta-

sandstone rocks ure sufficiently well exposed

near the E. & W.S, access road north of the

weir to place the inlier contact on the map

with confidence.

South-east of the weir the fnlier boundary

becomes involved in several tight folds—in

part interpreted previously as ua cross-fauh

(Mills 1963). On the ridge west of Wirrianda

homestead some good exposures of the un-

conformity surface may again be seen. Here

a coarse-grained muscovite and hacmatite-rich

schistose metusandstone overlies a chosely

folded mumuscovite-rich gneiss containing

quarizofelspathic layers and some haematite.

The unconformity surface is again seen to be

irregular in detail, Scattered pebble-like quartz

pods to 10cm in diameter occur in both the

basement and metasandstone and are ap-

parently of segregation ongin. Immediately

south of the homestead the haematite-rich

basal beds of the metasandstone run into the

Wirrlanda Thrust which marks the eastern

boundary of the inlier.

In conclusion, an unconformity between

rocks of the Warrea Inlier and the overlying

Adelaidean sequence is well established, The

inlier boundary can be mapped alung most of

its length with confidence, and details of the

actual unconformity surface can be observed

at two localities. The Jowest beds of ihe Ade-

laidean sequence are composed of schistase

muscovite-bearing nmvetasandstanes and the

basal beds are usually enriched in haematite,

although not as enriched as in ihe ML Bes-

semer sequence on ihe eastern side of the

neatby Houghton Intier (Miles 1950) A basil

conglomerate of the Jocal derivation has been

found wt onky one loewlity.

THE ADELAIDEAN SROURNCE

The siltimanite-muscovite zone

The lowermost units of the Adelaidean

sequence overlying the basement of the

Warren Inlier have reached the grade of meta-

188

morphism where sillimanite and muscovite are

in stable equilibrinm in rocks of appropriate

composition, Vhe basul formation is a thick

brows-hedded = achistose = felspathic metasand-

stone, which is overlain by a thick aluminous

peli Formution, “The top of this pelilic

formation has been cul out by mayor Caults

which have brought the sillimanite-muscovite

zone rocks into conjunction with tower grade

sequences. Three distinet phases of strong

compressive deformation have alfected racks

in the silimanite-muscovite yone and no re-

liable estimates of stratigraphic thicknesses can

be made.

The lithological character of the basal meta-

sandstone formation in Ihis arca has been

carefully described by Howechin (1906, p. 255;

1926, p, 5) whe noted its cluse similarity to

the Aldgate Sandstone, The mectusandstone

supports rather sparse vegetation and usually

forms large lcucoeratic outcrops. ‘Vhe friable

nature of this rock preserves the freestone

tchatacter of the Aldgate Sandstone despiic

high vrade melimurphism, Bedding, cross-

bedding and festoon-bedding, outlined by

laminoe of titaniferous haematite, are beauli+

fully) preserved although considerably ap-

pressed by subsequent tectonic deformation.

The haematite laminae ate normally about one

millimetre in thickness, but rare layers up to

10cm in thickness huve been observed, Miles

(1950) presents the results of a chemical

analysis of the ulaniferous haematite from at

specimen collccted in the northwest corner

of this area, In some oulcrops (eg, grid ref.

908070) the metasandstone is strongly mag-

nec; Magnetite presumably replacing the hae-

mate us the principal opaque accessory, H

is not known whether this magnetic propery

is confined to certain beds.

As described in the previous section, the

lowes beds against the unconformity are nor-

mally enriched in haematite, this component

being scattered evenly throaghout. These hae-

matite-tich beds are not mare thin a Tew

metres in thickness aid in roahy places they

thin ovt and disappear entirely, The next

30-50) tnetres of section consisls of a museo-

Vite-enriched metasandstone, perhaps best

desccibed os a quatlvamuscovite schist, The

remainder of the sectiun, perhaps amounting

ty SOO metres, consists of Selsputhig metasand-

stone, characterised by titaniferous hacmatite

Inminae outlining the bedding surfaces, with

lutenmitrent imuscoviteenriched layers. The

base of this mere qulittzofelspathic section

K. J. MILLS

was taken as the base of the psammutic forma-

tion oo my eurlier map (Mills 1963). As

desevibed by Howchin, rounded pebbles up Lo

30em in diameter, mostly of quartz or fine-

graihed gqualtzite. ace distributed throughout

the sequence, ullhough more commonly eo-

countered at certuin horizons, True conglo-

meratic beds are rarely observed, the pebbles

being mostly scattered unevenly on bedding

surfaces throughout the outerop. In some

exposures the pebbles are sten to have suffered

a strong flatlening and some elongation result-

ing From tectonism. Stratigraphic bedding can

usually be identified and opportunities for

facing observations based on cross-bedding

are numerous. Some slicing and transpasiiin

of bedding has heen woticed in the muscovite-

enriched section near the base of the stqtience

in. the South Para Gorge, Occasional pegmi-

tite and milky quartz veins carrying accessory

ilmenite plates Intrude the metasandstone

throughout the area.

Sixteen specimens covering the composition

range of the psammites were examined micro-

scopically. Quartz, ranging from 25-75%,

occurs in some rocks os Jarge strained clasts

up to 3mm. while other suniples, particularly

the qwore micaceous ones, demonstrate all

slages in the recrystallisution of original

strained clasts to new metamorphic grano

blasts. This recrystallisxtion is closely nsso-

ciated with the axial surface schistosily of the

second compressive deformation. In some

samples the new quartz grains preserve a pro-

nounced preferred orientation of their c-axes,

wppurently related to the second delormatiun.

Sume quartz clasis are sagenilic. Potash felspar

(0-30% } is the sule felspar component. It

usually occurs ax strained tartan-twinned cfists

up to 2 mm. In some specimens the clasts are

apparently untwinned but have partially re-

crystallised to small well-twinned pranoblasts

near their margins, Muscovite (S-50%) is pre-

sent in all specimens, usually as large flakes

vp to 2mm, commonly showing late strain

effects. It appears to be wholly of meta-

morphic origin and is. responsible for the pre-

servation of many of the tecionicully imposed

features of these rocks. Biotite is present in

many simples up to 5% and is usually pleo-

ehraic olive brown to pale lemon. Opaque

grains (1-10%) are invariably present. Apatite,

Zircon, monazite and tourmaline, pleochroic

pale pink to olive green, are accessories. Con-

sidering the coarse-grained micateous Entisses

above and below the schistose sandstones, the

STRUCTURAL GEGLOGY OF WARRTIN NATIONAL PARK

preservation of quartz and felspar clasts at

this metamorphic grade is quite remarkable

and the weakly metamerphosed appearance of

the more quartzofelspathic varieties of this

metasandstone miist be partly attributable to

the preservation of these clastic features,

The upper contact of the metasandstone

ligains! the overiying sillimanite bearing pelitic

schists is shaeply defined. In the south a thin

intermitient tremolite rock bed, aormally ex-

pressed at the surface as an opaline replace-

ment rock, tharks the cantact, while in the

east sume pelitic sehist is inserted between his

bed and the metusandstone, In the north-west

a sliver of coarse-grained sillimanite bearing

pélitic schist is observed to rest directy on the

schistese sandstone, The frue nature of the

tremolitie marker bed can be observed in

debris from a shaft sunk on the ridge nor.h

of Sailors Gully where the rock below the

weathered profile is composed of interlocking

pale-green trenalite-actinolite prisms, Else-

where the surface expression m an opuline

ohaleeduny showing tremolite casts and some

lale.

Vhe thick pelitic formation above this tre-

molite bed has been previously described in

some detail (Mills 1963, p. 171) These rocks

have auiicred intense folding and compression

and true bedding cannot be recognised with

cerluinty.. Although apparently quite thick, a0

estimites oO! straugraphic thickness can be

made. The socks are coarse-grained micucenus

schasts.ind gneisses, usually displaying alumino-

sificnte knots, tross-cutting crenulatiens and

small folds in their schistusity, leading to the

field name “crumpled schists” (c.g. Miles

1950), ‘The major primary constituents are

quarty, plagiaclase (An 0-15), biotite and

muscovile with variable amounts of sillimanite

and kyanile and rarer staurolite and garact.

Assemblages of these imtinerals developed in

rocks of appropriate pelitic composition and

approached equilibrium’ in a sillimanite-

Inuscovite grade metamorphic peak during the

second deformation, As wilh the basement

encisses, HO Metasomatism is considered to be

necessary for their formation. A pervasive

retrogression, which took place in the inier-

Kinematic periad between the second and

third compressive events, has resulted in the

extensive alteration of aluminosilicute minerals

and biotite to sericrte and chlorite. This retro-

gression is more pronounced in some zones

where shearing associated with thrust move-

muuts is belicved to have been important.

289

Some introduction of H.O may have secom-

panied this tetrogression,

fia the eust, part Of the pelitic formation has

been replaced by a hody of granite gneiss, as

pieviously described in greater detail (Mills

1963}. Although the chemical processes which

led to the formation of this granite gneiss are

hot yet understood, extensive chemical migra-

tions are not envisdged in its formation. This

eranite gneiss and its immediate envelope of

schists have escuped retrogressioa, Ti is en-

visaged that the granite gneiss body behaved

as @ sohd impermeable block durmg the reire

sressive cpisode which affected the adjacent

schists,

In Conclusion, the hasal metasandstones and

the woverlying pelitic schists have been sub-

jected lu a metamorphic peak in the middle

amphibolite facies under temperature condi-

lions where sillimanite was in equilibrium with

muscovite. Some clastic textures have been

preserved in the more quartvofelspathic meta-

sandstone beds but in the pelitic schisis exter

sive recrystallisution took place, Sillimanite,

kvanite, Staurolite and garnel were crystallised

during this. metamorphism aod grannisation

occurred Jogally, At a liter sige under yreen-

schist facies conditions. extensive relroyression

took phive in the pelitic schists.

The kyanite-andalusite 2one

A sequence of Adelaidean rocks belonging

to the lower amphibolite facies have been

(aulled against rocks ol the sillimunite-musco-

vite zone in the south, cast and north-west.

North of the Warren Reservoir, Alderman

(1942) placed these rocks in the bjotite zone,

a reasonable supposition considenng the abun-

dance of biotite-quartz-felspar schists which

oceur in this sequence. Aluminuus beds con-

taining undalusile or kyanite Knots are rare

and these koots are usually severely relro-

gressed jo sericite, Cale-silicaie beds in the

seqttence carry diopside, scapolite, amphibole,

epidote and oligoclase-undesine, confirming

their amphibolite facics character. This se-

quence of rocks is characterised in the field

by the fing to medium grain-size of the pelitic

and psammopelitic umnils and their stmple

structural character dominaicd by a single

schistosity, which in most outcrops is parallel

or nearly parallel to well-defined bedding

planes and bedding laminations. Crenulations in

this schistosity are rarely found, and if present

are weakly developed. The sequence ¢ast of

STRUCTURAL __MAP

OF THE

WARREN NATIONAL PARK

AND WESTERN POATION OF THE

MT CRAWFORD STATE FOREST

O00 ine Yet

UKAPRAINGA

Mine |

“

Boe

o-_

z —

RUST ASS

peek?) fl =

aa i 28

rae I aN

ey r vA s “

—=

STRUCTURAL GEOLOGY OF WARREN NATIONAI. PARK 291

LEGEND FOR

STRUCTURAL MAP

Lithological contacts _

oo a ad

Trends of bedding surfaces

Unconformity

Marker ‘horizons

Stratigraphic facing = we

-es tablished

—_—_—~

Foults ~inferred

-inferred

are

Thrusts

-established

Fault mélange ress

ADELAIDE SUPERGROUP

BEDDING eS = *

Sq Inclined Vertical Horizontal Inverted

FIRST DEFORMATION

\ Si, %,

5, LiBlg* Ls,

SECOND DEFORMATION

Sz 4, 52

S, LIBIg? \LIB)e?

THIRD DEFORMATION

% Sa S. Sa

Sy Xk LiBles Bg? L(B)e? \

BASEMENT

Compositional layering »

Schistosity *

Axial surface to folds in schistosity “s

Lineation in schistosity ™

Hinge lines of folds in schistosity

Fig. 2. (Opposite). Structural map showing the

principal structural features. in the region

around the Warren Reservoir.

the granite gneiss has been briefly described

(Mills 1963, p, 171).

Exposure of this sequence is very poor iin

the south and south-cast bul it seems that the

lowest unit is a pink meta-arkose containing

sorne haematite laminac, but no mica, and

preserving good clastic churaclers, South of

Watts Gully this meta-arkose is overlain by

a sequence of fine to medium-grained quartz-

felspar-biotite schists containing some pink

microcline-rich meta-arkose beds with acces-

sory pyrite. Then follows a tremolite rock

marker unit, expressed at the surface asa ten

metre width of opaline replacement rock. This

unit has been traced intermittently, using

exposures. of opaline replacement rock or talc,

around to the eastern side of the granite gneiss

where it forms a thick and useful marker

horizon. At the surface it is usually expressed

as opaline chalcedony, but fresh samples from

below the weathering profile consist of coarse

interlocking tremolite prisms. North of the

present area this same horizon is apparently

represented as a tremolite marble and has been

traced from well north of Williamstown to. the

proximity of the Warren Reservoir (Howchin

}926, pp. 7-8; Hossfeld 1935).

East of the pranite gneiss the tremolitic

marker unit is overlain by a mica:schist group

consisting of fine to medium-grained quartz-

felspar-biotite-muscovite schists with thin inter-

bedded meta-arkoses, Most of these meta-

arkoses are fine-grained, pyritic, graphitic and

very enriched in microcline. A useful pink Sels-

pathic quartzite marker horizon crops out

persistently a little above the tremolitic marker

unit. Some mica schist beds contain small

knots which have altered to fine sericite. Rare

kyanile relics have been found in these knols.

The uppermost part of the sequence examined

is a Calc-silicale group consisling of inter-

bedded fine to coarse cale-silicate rocks and

knotted fine-grained mica schists.

A wedge of rocks belonging to the kyunite-

andalusite zone has been mapped west of the

Ukuparinga Copper Mine, in the north-west

corner of the area. The lowest bed here is a

thick medium-grained dolomitic marble, which

may be equivalent to the tremolitic marker

bed east of the granite gneiss. Specimens of

this rock consist largely of dolomite with

variable amounts of tremolite, talc, muscovite

and primary chlorite. Calcite is rare or ubsent-

‘Two. analyses of this marble are presented by

Miles (1950), This marble is overluin by a

mica schist sequence, containing fine-grained

242 K. F. MILIS

pyritic meta-arkose beds, very similar to that

east of the granite gneiss. Higher in the

sequence some mica schists have sericite knots

containing andalusite relics. The cale-silicate

group has not been recoguised here, although

a second marble unit crops out high ia the

sequence against the Williamsiown-Mecudows

fault.

Biotite zone

No attempt has been made te map beds in

the low grade sequence expasedl west of [he

Williamstown-Meadows fault. Near the [fault

the main rock types are fine-grained grey

dolomites, grey-brown dolomitic phyllites,

phyilitvys and fine-grained quartzofeispathic

pyritic metusiltstones. Rocks of the biotite

zone sre usually extremely fine-grained

(0.01-0.03 mm). A pale mustard-brown weakly

pleachraic biotite is characteristic of the phyl-

litic tocks. Dolomite seems to dominate over

calcite in’ the carbonate rocks. A thick

sequence of grey impure dolomite; (20%

quartz, plagioclase, muscovite and opaque

impurities) is exposed south af the South Para

River

CONCLUSIONS

‘The basement rocks of the Warren Inlier

are Wnvenformably overlain by the Adelardean

rocks. The Adelaidean sequence is divided into

three portions belonging to different mela

morphic and structural levels by several major

fault surfaces, The basal sillimanite-muscovite

zone rocks and the kyanite-andalusite zone

tocks of the Adelaidean sequence are sepu-

rated in this. area by Faults which ate surfaces

of marked metamorphic and structural di-

continuity. It therefore seems likely that there

is a large stratigraphic gap between the

Sequences represented within these meta-

morphic zones, Further detailed mapping, par-

ticularly to the north of the present area, may

help to determine how much of the struti-

graphic sequence has been removed. Until this

problem is solved it seems unwise to attempt

correlations of individual beds or parts of the

sequetice with other beds or sequences in the

Mt. Lofty Ranges. The Williamstown-

Meadows fautt brings biotite zone rocks in

the west against sillimanite-muscovite zoue

rocks. As suggested by Miles (1950) the biotite

zone tocks probably belong to a much higher

stratigraphic and metunwrphic level in the

Adelaidean sequence and displacernent on this

faull must be very large.

Structural Relationships between Mapped

Lithalogical Units

PRELIMINARY COMMENTS

Three successive compressive deformation

events, Fi, Fe and Fs, have affected the Ade-

Juidean sequence in the vicinity of the Warren

Reservoir and the structural features produced

in these de‘ormative phases will now be

described more fully. Metamorphism of the

Adelaidean sequence began betore or during

Fy and reached a peak temperature in the

amphibolite facies early in the Fy episode.

A series of east to west thrust movements

occurred Jale in the F, event and extensive

Telrogression under greenschist facies condi-

fens accompanied or followed these moye-

ments. ‘Uhe thrust sheets were folded during g

Tather hrittle low temperature F, event. After

F, and late in the cooling history the Williams-

town-Meadows fault developed its maximum

displucement,

In describing the struelural features and

events in the Adglaidean scquence it is cane

yenient to introduce the following shorthand

nojatian? (see also map legend, Fig. 2)—-

S) —surface of compositional

layering relating to pri-

maty bedding.

F,, Fu, F, --the three successive

compressive events.

S,- Su. Sp —axial surlaces to fulds

produced in the F,, Fa,

F; events respectively.

—fSulds in bedding with 8.

as axial surface etc.

—lineations resulting from

Sp-Sy intersections etc,

—strain elongation axis in

Sy ete.

Orientation measureinents are recorded in

telation to true north-point azimuth. Figures

2 and § illustrate the principal structural

features

B(Sp-So) ele,

L(Sy-So) ete,

LiS,) ete.

THE BASEMENT (WARREN INLIER)

At the type locality of the basement rocks

at the Warren Reservoir Weir a partial history

of tectonic events may be dcicrmined. As in

all exposures of the basement rocks, bedding

2 Owing 10 ptinting difliculties this form ef notation is adopted im the cext cather than ths more

conventional form shown on the map Jegend.

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

with stratigraphic Significance cannor be

proved, although quartzofelspathic bands and

layered lithological Variations may reHect 4

primary bedding precursor. Lithological layers

and schistosities in Ihe expusures near the weir

are strongly folded on all scales and at first

sight the folding appears to be rather regular

wilh a prominent schistosity. defined by

course mica plates, crenulated and folded

about shallow plunging axcs (Mills 1963). This

schistosily is observed in detail to be a highly

evolved crenulation cleavage, and is therefore

an axial surface schistosity belonging io at

least a second deformation event. In paris of

this exposure this schistosity has been folded

into recumbenr Z-shaped folds with near hori-

zontal hinge surfaces, and these folds have

been overprinied in turn by a widespread later

folding with a moderately west-dipping axial

sutfuce, produging ¢renulations in the earlicr

schistosuy with ow wavg¢lengih of O,5-3 cm,

Thus, at least four overprinted fold even's

can be distinguished in this exposiire, and

there are yet other folds present which may

represent a lifth deformation. The earlier faleds

in the weir exposure tend to huve a. ptygmatic

style in which the fold hinge lines have a more

regular orientation than the hinge surlaces,

Nevertheless, the hinge lines remain curvi-

linear on all scales and the folds are never

strictly eylindrical, The Jater folds are also

irregular and often of polyclinal siyic, this

being puriistly induced by the presence of

many large intrusions of pegmatite and blocks

and lenses of quurtzolelspathic gneiss which

have acted as. buffers inducing inhomogeneous

strain during the later fold movements (Fig,

3b, c, e). Due to these irregularities, reliable

field? measurements of the orientulion of siruc-

tural elements are difficult to make, even in

the most favorable exposures.

Lisewhere in the inlier most exposures show

signs of complex folding and overprinted de-

formation structures, justifying field names such

as crenulated or crumpled schists. Bedding

cannol be veriligd and any lithological layering

present is strongly lenticular und suggestive of

Irunsposition processes, Sone exposures are

very irregularly deformed and tio orientation

measurements can be made, but some of the

more micaceous schists display fairly regular

folding of their schistosity, approaching local

cylindricity, There ts much variation in the

style of small folds from concentric to shar}

chevron folded forms (Fig. 3a. dc. fi). Most

pegmatite intrusions have alse been folded

243

along with the host rock schistosnies.

Examination of exposures in the vicinity of

Lookout Tower Hill agam suggests multiple

deformation involving at tcast four conipres-

sive eVents, the Jutest phase involving ubi«

quitous tight to ope chevron style folds in

the earlier schistosily of the more micuccous

rocks.

Microscopically the basement socks are

cuoumegrained, wilh a prominent schistosity

defined by oriented mica flakes, which are

oflen segregated into Jensoidal gneissic layers

with signa of evolution thtaugh an earlier

crenulation cleavage stage. In parts of the

inlier a strong mineral fineafion, detined by

sillimanite fibres in aluminous schists or mic

plate dimensions, 18 observed within the <chis-

tosity, Folds and ercnulations in the schis-

(osily are ubiquilous and are mostly pre- or

synmutamorphie. Some ot these lolds seem to

be closely related to the F.,, deformation in the

overlying metasandstones. Weak Tate meva-

morphic strain features, undulose extinction

und deformation lamellae in quartz and kink-

ing and bending of mica plates, are observed

In Most specimens,

Although some structural measurements

have been made in the basement rocks (Fig. 6,

Sub-areu Aj, these have little or no meaning

in terms of the complex structural history 14

which these rucks hive been subjected, and 4

more complete understanding of their -struc-

tural history may. only evolve through a more

detailed structural analysis of the whole inlier,

‘THE ADELAIDEAN SR@URNCE

Yhe sillimanite-muscovite zane

The busal unit of the Adelaidean sequences

is & schistose metasandstone in whith quartzo-

felspathic and mica-rich layers and titaniferous

haemittite Jaminae clearly oniline prinnury

bedding (So), and well preserved cross-beddiing

structures provide evidence for strahyfaphic

facing as described previously. Plates of white

mica, presumubly crystallised from a former

clay/felspar fraction in the sandstone, ate

present in almost all beds of this unil but

become more abundant towards the base.

‘These platy crystals have enabled various tce-

tonic structures to be preserved m the aeta-

sandstone, and [rom a study of the mica plate

orientations a lectunic histury ¢an be erected,

Like the overlying pelitic scquence the basal

meétasandstones have been ifected by three

major deformative events F,, Fy, and Fy

(Pig, 6). The F; ond F, events caused tight

794 K. J. MILLS

folding of the mctasandstone throughout most

of the area considered here. The Fo event in-

volved sirong compressive deformation near

the peak temperature of metamorphism and

this combination has tended to obscure the

effects of the F; event im most exposures.

During the Fy event a strong S$. schistosity

evolved through the crehulation and trans-

position of an earlier S, schistosity. The effects

of the Fy event are rather weak and are

responsible for some post-crystalline crenu-

lations in, earticr schistosities in the centre of

the area and macroscopic folding of earlier

structures in the south-east (Fig, 6, sub-arcas

M, N, 0, P, Q).

Most cxposures of the metasandstone: dis-

Play a schistosity defined by oriented mica

plates. In the less micaceous rocks same

difficulty is experienced in differentiating this

schistosity as S, or Su. In some of the more

micaceaus tocks S,; and S, are both present

and can be clearly distinguished on the basis

of overprinting relationships, Where S, is most

clearly preserved it is seen to be defined by

well-oriented mica plates. The mica crystals

are grouped into anastomosing clusters of

nearly parallel plates separated by a single

Jayer of quartz and telspar grains. The clusters

are evenly distributed rather than forming the

segregated trains of mica plates more charac-

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

lertstic of The Sy microstructire, The gram size

of the mica plates does not seem lo be a

consisicnt leatyre for the distinctian ef §,

ant S.. In situations Where (te S, surface lies

at a distinct angie to Sp and in cross-bedded

micaceous melusiodstunes, S, can be shown

to be an imposed tectonic feature and not a

“bedding foliation”, However, in most out-

crops 5, is sensibly paraliel to S,, suggesting

a position on the limbs of very appressed F,

Falds,

Owing to the strong overprinting effects of

the Fs event, inacroscopic F, folds cannot be

readily mapped oul, but the shape of the base-

meal exposure sugvests the position of some

macroscopic F, folds, A stereographic plot of

poles to bedding surfaces measured over the

large synclinal structure straddling the cenire

of the inher results in a broad girdle pattern,

the pole of which, plunging ut 20° towards

202°, may be laken to represent the mean

macrascopic B(S,-S,) fold axis for this strne-

ture (Fig, 4, sub-area L), The orthographic

block diagram of Fig. 8, showing the general

form of the stnicture, has been derived using

this calculated H, uxis and the local orienta-

tion data on the overprinted F, and Fy struc-

tures. In the north-west of the area, for

example along the Engineering and Water

Supply track crossing lhe metasandstone on

the western side of the inlier, same mesoscopiz

F, folds show tight appression wiih ihe 8,

axial surface structure striking 002° and dip-

ping steeply eastwards. Insufficient observa-

298

lions have been made bo discuss strain in the

PF, deformation,

AML stages in (he Gevelopment of the S.

Stvucture can be observed in the metasand-

stone, from faml, open crenulations in the

earlier S, schistosily, to uppressed crenulativns

in which the mica plates have become con-

centrated in the limb regions, leaving. (he

hinge areas enriched in quartz and felspar with

only a few diversely oriented mica plates; to

& new gneissose schistosity in Which the mica

plaies are largely segregated into trains

parallel to So, leaving little sigu of the previous

S, structure in the rock. In the more quartzo-

felspathic beds both the quartz and lelspar

grains have discoidal shapes with Jong axes

lying in the Sg surface, The mica plates defin-

ing the crenulations of the new S. schistosity

characteristically lack pronounced — strain

features and evidently underwent recrystallisa-

tion during and after the Fy, event, that is

syntectonic and podst-tectonic crystallisation,

and ihis feature serves to distinguish F,, crenu-

lations from Fy crenulations over most of the

area, However, in the south-western portion

of the Warrén National Park detormation in

the Fa event outlasted recrystallisation. Here

mica plates huve been strongly kinked and

intragranular movements outlasted strain

relieving processes. Relict quartz clasis shuw

strong wndulose extincnion with deformation

bands parallel to S, and newly crystallised

quartz grains have developed a pronounced

caxis fabric during the F. event. This fabric

Fig. 3, Structures in basement rocks of the Warten Inlier and at the base of the Adelaidean succession,

a—Prulile of folds in coarse-grained quartz-mica gneiss, Warren tnlicr, A well developed

gneissic schistosilty has been thrown into regwiar chevron folds ina deformation: which may be

correlated with Fs in the overlying Adelaidenn succession, Traced from photograph. Location

918098.

h,—Profile of folds in basement rocks, Warren Reservoir weir. Quartzofelspathic layer in mice

unecixs stuwing polyctinul folds. A crenufation cleayage cross-cuts the folds (shading) aad

crennlates an earlier axial plane schistosity in the mica gneiss. Freehand sketch, Location

916116,

c and ¢—Disharmonic folding of quarizofelspathic layers in coarse-grained mica gneiss, Warrett

Reservoir weir, Small folds associated with the crenulation of an earlier schistosity show 2

polyclinal style. Traced from photographs. Location 916116,

d.—Profile of open folds in course-grained mica gnedss containing thin quartzofelupathic luyers,

Warren Inlicr, ‘raced from photomicragraph.. Lacation 928098, ,

f. Sketch of unconformily between basament rocks of Warren Inlier and basal motayandstone

of Adeglaidean succession. Drawn looking eusiwards. The quarizufelspathic basement (stippled)

has thin ovitaceous layers dipping al a low angle to the south. The gaconformity is steeply dipping

but has an irregular detailed topography, A hacmatite-rich mic¢uceous. metasandstone showing

traces of bedding in the form of hacmatite-rich seams (fine stipple) is welded onto. the base-

ment und has a strong S, schistosity, delined by the orientation of mica plates, dipping to the

south (shading), Freehand field sketch, Location 912091, Warren National Park,

“—An angular quarts pebble immersed in coarse-grained Muscovite-rich melasaadstone near

the hase of he Adelaidewn succession. Note the Fy crenulations im the earlier S$, schistosity-

Vraced from photomicrograph. Location 908107.

f.—aAn example of the uverprinting of carly folds in schistosity of a quariz-muscovite gneiss

by later folds, Warren Tnlier. Sketched from hand specimen, Location 917106,

296

has not yet been investigated in detail, but

appears. 16 involve a girdle or crossed girdle

pittern in which the cakes tend to be sym-

metrically disposed to the Sy surface and iu

the strony L(S,-S.) lincanon lying within jt,

A lineation, L(S,-8.), is scen to lic in the

S. surlace in most exposures throughout the

area. Where 3, is developed only as a crenu-

lation cleaviize this lingation is the crenulation

axis and is the geometrical result of the inter-

secion of the §, and So surfaces. Where

Sx is more strongly developed into a new

schistosity the lineation may take the form of

a mineral streaking effect on the S. surface,

Microscopically this. mineral streaking is seen

to be the visible effect of elongate mica putes,

with variable dimensions but averaging 1:5710,

whoch are inutuzonally arranged about the

lineation axis with their longest dimensions

parallel to the lineation, Some quartz and fel-

spar grains are also elongate parallel to ihe

lineation. Quartzose pebbles are often discard

within S, and slightly elongate parallel to the

lineation, However, whether this Jineation,

which hax heen mapped as an S,-S, inter-

section lineation in the field, is alsa a principal

axis of strain has not yet been determined.

Most of the mapped macroscopic folds

within the metasandstone and involving the

unconformable contact between the metasand-

stone and the basement rocks have proved lo

he Fy folds. Mesoscopic F, folds in both

bedding and S, surfaces are not uncommon.

Two small B(S,-S.) folds from nomh of the

well, illustvated in Figs. 4a and 4b, were

analysed using the technique sugycsted by

Ramsay (1962; 1967, p, 413) for unravelling

flattened flexural slip folds. In both causes the

western lintbs proved to be more “‘flatiened"

than the eastern limbs, und a mure micaceous

layer had both limbs “flattened more than

100%", These resulls are unrealistic and

indicate that olher mechanisms besides flexural

slip and flattening were involved. The grealer

“flattening” of the western limbs could he

explained by a component of simple slip or

sheacting motion, involving intergranular

movemeits, which would be consisient with

the enst to west thrusting movement charac-

teristic of the laler stages of the F. event.

In the incompetent micaceous layer mass

movement of material from limbs 10 nose

could explain the anomalous “fiattening" in

these layers. However, 4 more generalized

mechanism may have heen responsible for

these folds (Hobbs. 1971),

K. F. MILLS

In the vicinity of 906093, crenulations with

a Wavelength of 4-1 cm are seen to huve hinge

surfaces parallel to those of farger folds.

These hinge surfaces suike at 335” and dip

steep westerly and are interpreted as belong

ing to F, folds. In some specimens L{S,-S.)

lineations ace seen to be folded over these

crenulations, Thin sections show that all

crystals have preserved intense strain features

related Jo this deformation, In the south-vast,

in the vicinity of the Gumeracha Goldfielkts,

struclures in the metasandstone have been

folded aver a large Suuth-easterly plunging F,

anliform,

In thin section, specimens of the metasand-

stone from throughout the area show some

strain in the quartz and mica crystals, but it

is not known whether this is reluted to the Fa

deformation event outlasting reerystallisution,

the F, event, or some other luter mild phase

of deformation.

Rocks of the thick pelitic sequence over-

lying ihe basal metasandstones are charac-

terised by a coarse gtain size, a pronounced

schistosity defined by mica plates, and an

abundance of mesoscopic linealions and lold

structures. Like the basement gneisses, there

is much variation in the textural and sirucg-

tural features of each rock depending on the

original composition and the Jocal tectonic

history. Figures 6 and 7 summarize the meso-

scopic orientation data measured in the Ade-

laidean sequence, Similarities in the orientation

data measured in the metasandstones and

overlying schists und gneisses may be noted

(e.g. cumpare sub-areas R ind H with sub-

area J).

The most attractive structures within the

pelitic schists are the open tu moderately tight

mesoscopic folds belonging to the F, event,

These folds show varying degrees of develop-

ment in different oulcrops and are apparently

ahsent in some parts. The style of the F,, folds

and their patchy distribution suggests that they

were produced in a rather mild Jale lestonic

event when compured with the intensely bonm-

pressed nature of the carier siructires. The

main schistosily in these rocks can be observed

to be an axial surface slructure to very ap-

pressed, almost isoclinal, folds and to be a

highly evolved crenulation cleavage belonging

fo the F., cvent. No mesoscopic F, folds have

been identified in these schists, although relics

of an earlier schistosily testify to the presence

of a possible axial surface structute, equrva-

STRUCTURAL GEOLOGY OF WARREN NATIONAL PAKK

lent to slaty cleavage, for this earliest tectonic

event,

No bedding with stratigraphic significance

has been proved within these schists, Len-

ticular’ compositional layering, labelled $,. is

observed within the larger exposures, but even

this thickest layers are not traceable as bedded

units, Attempts to map out lithological unite

ona larger scale, using compositional and tex-

tural variations, have failed. This could be

partly cue fo luck of silicient continuous

exposure, Relics of an carly schistasity, S;,

presumed tu be wn adial surface structure for

the F, event, are to be found in many expo-

sures, These relics take the form of an early

schistasity acting as the folded surface in

some woclinal Fy folds, which are usually best

preserved in rocks of more quuttzase cam-

posilion, and relics of an early crenulated

schistosity in microlithons within the F.

microstructure in rocks of more micaceous

composition. The observalion of disc-shuped

quartz-sillimanite and staurolite knots lying

within the S, surface forming the folded sur-

face of F, folds suggests thar these minerals

erew during or after the F, event and before

the imposition of the Fe event. No B(Si-S1)

foids have been identidied in the schists. From

the secant evidence available it seems that 5,

and S, were nearly parallel in these rocks,

and this could be attribulable to a sitwation

on the limb of a large appressed F, fold.

The mai schistosity in these rocks, Ss,

lonms the axial surface structure to tight folds

produced in the Fy, event. In some exposures

relics Of appressed crenulations in S,; with

sharply attenuated hinges are observed within

the §, microstructure. but transposition of

the earlier schistosity has been so great that

only rarely are these crenulation hinges. pre-

served, The more fully evolved S. micro-

structure is characterised by w coarse-grained

gntissic texture in which quartz and ftelspar

granoblasts are sezregaled into thin lenticular

plates interleaved with trains of coarse-grained

mica Makes. Mies plutes comprising the mica

(rains commonly show a consistent imbricate

Or echelon stuckiny arrangement indicative of

an evolution of the Sy microstructure through

the concentration and metamorphic segrega-

fon Of a pre-existing $, mica preferred

orientation (Fig. 4g). Isolated mica plates

withic the quurtzofelspathi¢ Jenses tend to

show a diversity of orientation, Where un-

affecied by the Fy event the So surfaces in

297

tocks south of the reservoir have a mean

strike of 350° and dip 75° east.

Fulds in compositional layering and 5,,

with S. as axial surface, are not vncommenty

met with, bul are less obvidws than the later

steep plunging F, folds. These F. folds are

tightly appressed and almost isoclinal with

thickened hinge regions (Figs. 4c, d, c, fy

They are overturned to the west and ther

hinge lines plunge at variable angles. within

Sq. The strong S, axial surface structure tends

to obliterate the folded S, surfaces, especially

in. rocks containing coarse porphyroblastic

knots, A strong lineation L(S,-S,) results from

the intcesection of the 5S, and Sy surfaces, This

lineation takes the form ol a mneral streaking

or rtodding defined by ellipsoidal shaped

granoblasts and mica plates, or is more rarely

Aven a6 crenulation hinge lines. The lineation

is usually parallel to the axes of Fa lolds itn

S) or S,, bul examples are known where the

lineation is more steeply plunging than

B(S,-S2) fold axes, suggesting that S, and S,

were not sttictly parallel before the Fy,

deformation vent. Near the old reservoir

rouwd bridge the L(S8,-S,) lineation has a

shallow north or steep casierly plunge, bul

further south und west a moderate south-

easterly plunge becomes predominant, Cross

joints have been developed perpendicular to

this Imeation. It is not known to what extent

this lineation is also a principal axis of strain.

A mild Fy event occurred lute in the meta-

morphic history producing patchily developed

open to tight F, folds, These folds are mostly

B(S.-S,) folds, but locally B(S,-S,) and

B(S,-S,) folds may be found. Several

examples of the overprinting of Fy folds on

F, folds have been observed, The F; folds

usually have open concentric, boxlike or

V-shaped styles, which pass into regular or

polyclinal chevron falds in the more strongly

deformed exposures | Fiz. 5). Mesoscopic folds

near the reservoir haye wavelengihs up to

6 metres, but much larger macroscopic folds,

auch as the Gumeracha Goldfields antiform,

occur in the south. A mapped macroscopic.

told in the south-west has a curious irregular

form in which S, has been folded about ah

axis plunging 20° to 153°, but the F, struc-

tures show various. anomalous -orientutions.

B(S.-S;) folds plunge steeply north-cast to

south-east near the reservoir (Fig, 7) und

moderately south-east in the Warts Gully

region (Fig. 6). Rotation of earlier L{S\-S,)

lineations in conical surfaces Suggests 4

288 K. J, MILLS

Fic. 4-

STRUCTURAL GEQLOUY OF WARREN NATIONAL PARK

fexural slip mechanism. The Fz folds tend to

split alang their hinge surluccs on exposure

and this is ofterr the only expression of an

Ss wxial surface structure. However, in the

tightest F, folds an S$, crenulatwon cleavage

has begun 16 appear, Fy folds tend to have a

polyclinal style with considerable variation in

the orientation of their axial surtaces, Neal

the reservoir the Fy folds have a left-handed

vergence and §., axial surfaces vary tn strike

from NE-SW for open fold styles. to N-S for

appressed styles where the S; crenulation

cleavage has begun ta appear (Fig. 7). In the

Wults Gully tegion the folds have a right-

handed vergence, the S, axial surfaces in the

open folds having a NW-SE strike swinging

1o N-S as the folds become tighter (Fig. 6,

sub-sreas M, N, O, P, Q). Under the micro-

scope lhe F, folds near the reservoir seem

to show a greater degree of healing of both

quartz, and mics in their hinge tTegions than

do Fy folds in the west and south-west of

the area, ‘Thi may suggest a slightly higher

lemperatute during the Fy event in the

vicinity of the Mount Crawford granite gneiss.

There ure a few exposures in which measure-

ments made On late fold siructures suggests

anomalous unentations. for example, the irre-

gular syniorm in the south-west, These

anomalies muy be related to a conjugate P;°

arian Fy event,

The Mount Crawford granite gneiss replac-

ing the eastern part of the pelitic sequence

contains a pronounced schistosily with the

299

charagtenstic gneissic S: microstructure of the

pelitic schists including the characteristic im-

bricate stacking arrangement of individuil

mica plates within the mica trains. A strong

lineation, considered to be L(S)-S.), bies within

the schistosily and is defined by elongate mica

plates and quartz and felspar grains, The

schistosity has a mean strike of 349° and a

dip o! 56° east and the lineation plunges 33”

to 149° (see Fig. 6, sub-area G), The unitonn

orientation of the L{S,-S.) lineation t related

to Lhe uniform initial orientation of S,; and 5S.

and the fact that the granile gneiss has largely

escaped the F, deformation event. The granile

goeiss would appear to have behaved aos a

solid block after the main metamorphic. peak

was teached early in the Ps eveni. As a con

sequence it has escaped the lale or post-F

relrogressive event and the effects of the Fy

deformation. Skialiths of pelitic schists within

the granite gneiss have becn affected by the

F, and Fy events, but not the F, event,

Numerous amphibolite dykes of basaltic or

doleritic parentage have been mapped in this

area (Mills 1963), (hey ate confined to the

coarse-grained schist sequence east of the

Warren Inlier and also penelrale the granite

gneiss. They have a distinctive microstructure

made up of a schistosity and strong lmeation

defined by hornblende prisms. Within dykes

cutting the granite gneiss these slructures are

concordant with the S.-L{S,-S.) microstructure

of the enerss. Within the pelitic schist sequence

both Fy and F, falds have been observed

lig. 4. Profiles of F: folds in Adeluidean succession. ;

uw. and 6—Moderately light Fy folds in metasandstone. Note Ss crenulation cleavage deforming

earlier 8 schistosity in mica-rich layer in a, and weak So axial plane structure defined by flattened

quartz grains and ortented mica plates in &. Traced trom photographs, Location 917126.

c—Tith! Fo folds in quartzofelspathic layers (stippled) in micaceous gneiss of the thick pelitic

sequence, Nate thut an early schistosily ($1) preserved in the quartzofelspathic layers patallel

in the layering is folded in the Fy deformation. In the micaccous gneiss the 5. crenulation

cleavage has been Jargely transposed into a new schistosity, Traced from photograph, Location

28116,

d— FE. folds in quartz-felspar-sillimauite-mica gneiss of the thick pelitic sequence, An early S,

schistosity, apparently parallel to the prim

ary compositional layering, is almost obliterated by

ihe imposition of the S, cleayage axial plane to the folds. Traced from photograph. Location

92ST.

¢, and {Tight F. folds in coarse-grained mica schist containing quanizofelspathic layers (quartz

stippled. inica shaded). An earliet schistoslty (S,), outlined by mica plates, is well preserved in

both mica-tich and quartz-rich layers (S.). Traced from photomicrographs. Location 934094.

ge—Tracing from photomicrograph showing early stage in the development of Sy mica-rich

layers during the process of crenulation of earlier schistosity (S.) im a quartz-biotite-sillimanite

achist enclave in the granite gneiss, In the granite gneiss the S, structure 1s largely desiroyed but

ihe Se gneissasity commonly preserves the characteristic echelon or imbricale arrangement of

mica plates. Location 939102,

A—E: folds in fine-grained quartzofelspathic bedding laminations (stippled) in doloritic

phyllite. The axial surface structure in the phyllite is a very fine crenulation cleavage (shaded),

Wote the cross-cutting quartz veinlets which were ptygmatically folded in the Fz deformation,

Biolite zone phyllites west of Williummstown-Meadows Favtr-

Location 890120.

Traced from phoiomierograph,

)

— AF

Sey (gs

—_——_

a a

—

(Miah

(TY

yates iy

i aE Hi Uf!

pbs

fo" tf!

Yess

eens

K. J. MILLS

‘

ed)

y; yy

oO i /

if}

3] t/

300

‘

Fig. 5

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

within the amphibolite dykes. Some Fy folds

involving amphibolites have been recently

exposed on the south side of the reservoir in

the cutting for the road leading Lo the new

bridge. The amphibolite: were apparently in-

truded during or prior to the F, event.

Veins and pods of pegmatite and quartz

are intruded extensively through the pelitic

sequence, Some of these were strongly sheared

prior io the F, event and were subsequently

folded in the Fy and Fy events, but most of

the coarse-grained massive varieties appear to

have been intruded after the Fu event, Some

of the smaller pegmatite veins were folded

during the F, event. Some large tourmuline

porphyroblasts were observed to have grown

across Fy ‘structures,

The kyanite-andainsite zone

Medium-grained biotite-quartz-felspar

schists, marbles and cale-siheate rocks belong-

ing to this zone are exposed cast and south

of the Murray Vale Thrust and between the

Ukaparinga and Williamstown-Meadows faults.

in the north-west. The schists in this sequence

ure characterised by a simple planar schis-

tosity, S;, made up of oriented mica plates

which ate usually evenly dispersed through the

rock, This schistosity is almost parallel to

bedding laminations in most exposures and no

mesoscopic er macroscopic F, folds have been

found. Deformation structures Telated to the

F,.and Fy events are rarely observed und are

only weakly developed. A notable coarsening

of grain size, especially of mica plates in mica

rich laminae. and the growth of post-tectonic

muscoyiie porphyroblasts occurs low in the

sequence udjacent to the higher grade block

and near pegmatite intrusions. This could be

due to some kate contact heating aller thrust

sheet emplacement. Peymiutite Intrusions of a

massive or zoned type are rare and are con

fined to a few veins running parallel to S.

immediately east of the Murray Vale Thrust,

No amphibolite intrusions are known to cut

rocks of this zone,

Bedding, defined by compositional variation,

is well preserved on all scales in this sequence

and where the exposure is sufficient the beds

are found ta have great lateral continuity.

Stratigraphic facing indicators are rarely

observed, but the sequeuce is considered to

dip east and to face east in the east and to

dip west and face west in the north-west

block, the two wreas of exposure representing

the limbs of a very large F, anticlinal struc-

ture. The schistosity S,, assumed to be axial

surface to the mucroscopic F, structure, is

observed to lie at a smal! angle to Sy, usually

less than 10° in the more micaceous rocks.

This tends to promote splitting along ihe

bedding surtaces of the quartz-felspar-biotite

schists to yield slabby blocks which were ap-

parently favoured for building purposes in the

early days of seitlement. Microscopically the

5, surface in the schists is defined by the

orientation arrangement of biotite plates,

which tend to have an even spatial distribution

except in strongly knotted schists. where cus-

pate concentrations of biotite plares have

grown at the margins of porphyroblasts. ‘These

porphyroblasts are mostly retcogressed to fine

sericite but contain rare telics of andalusite

und kyanite. The size of inclusions in the

Fig. 5. Profiles of F, folds in the thick pelitiy sequence of the Adclaidean succession,

a—Open Fs folds in mica schist, The main schistosity (S:) is apparently parallel to the com

asitignal layering. Sketch from photograph. Location 928117,

_—Polyclinal Fy folds in mica schist. Main schistosity ix Se Fs fold outlined by quartz fens

has been folded in the Fy deformation. Traced from photograph. Location 926116.

c—Open Fy folds in micaccous metasandstone, Main folintion is S:. Traced from photograph,

Loeation 924109.

d—Open F- folds in miva schist. Main schistosity is S. which appeats to he parallel to the

quartzofelspathle fayer at the baxe of the diagram (stipplei)-

Traced [rom photograph, Location 926117,

Note cross-cutting quartz lens,

e—Tigm F: folds in quartz-felspar-mica gneiss. Main schistasilty is Ss Traced from photo-

micrograph, Locution 929119,

{—Disharmonic Fy folds in mica-quartz gneiss (quartz stippled, mica shaded). Main schistosily

is Ss, Note late cross-cutting fault. Traced from photomicrograph. Location 918060.

v—tTieht F, folds in quiarlz-muscovile gnetsy showing incipient development of Sy crenulation

vleavaze (quartz stippled, mica shaded).Main schistosity i5 S:. Traced from photomicrograpls,

Location 943118.

* Owing to differences in the structural development in the high and low-grade sequences thecorrelalion

of mesoscopic structures is p mutter of conjecture, The author has adopted the simplest correla-

tion campatible with his present knowledge of the area.

302 K. J. MILLS

SUBAREA E 5

| 35. 4 LIBS: 4

Soc

2 Lal?

= L Lge

ere ARES F

a Se

‘ “—

{

SUB- aes G

251 Sz

i vine)

[Max 6Bur

198 LSe

imax da-laa; Se

| - SUBAREA, H

ul _—_

ao,

SUBAREA A (BASEMENT)

58 SCHISTOSITY 6 MINERAL STREAKING | 25 AXIAL PLANE 32 CRENULATION

PLANES = LINEATIONS o CRENULATION po, LINEATIONS «=

CLEAVAGES * a mA

Fig. 6.

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK 303

Soe S,+ Lipa “ S:: Lisig2

Leis»

SUB-AREA aw

1 Lips

SUB-AREA K

4 LIBIS: | 15 So 1 Ss

la LE Nop |

SUB-AREA L

11s, F 87 S {7 LB) 18 Sy

7 A nape 2 3 Lil: a4 LieySs

SUBAREA? « MN

\ Lyeyg2

SUBAREA: s OPQ adh

13 Le oe 2 LIBlgs |

Fig. 6, Lower hemisphere equal area projections of structural elements measured in all sub-areas shawn

in the inset figure except sub-area R, True north at top of diagrams. Contours at 0.5, 5, 10, 20,

30% per 1% area.

304 K. J, MILLS

Na ees

RESERVOIR

DMO Ih

FINE-GRAINED

MICA SCHISTS

METASANDST ONE

bad WARREN

INLIER

Ss > Se

SUB- a, * LB)! a S, LiBIee a

AREA L(B) 3? *

xe ‘Sh Sz

35, pot i L(Big! | 64 Sz 2 L(ahge

F2-072)

34 LIB)SS

(MAX GO-O701 42

/ ;

R {

| A ae 25 Lip) Ss 33 LBS

: (Max. ¢5- 058) z

72S, 172 3;

(MAK (wax,

fa— 2a)

Ro te

109 .(B)$

| \MaAwe at 's

Fig. 7. Lower hemisphere equal area projections of structural elements measured in coatse-grained

Adelaidean schists of sub-arca RK. True north at top of diagrams, Contours at 0.5, 5, 10, 20.

30% per 1% area.

STRUCTURAL GEOLOGY OF WARREN NATIONAL

porphyroblasts jo relation to matrix grain size

indicates gerowlh during and after the F,

Ueformation event. In other rocks ellipsoidal

quartz, felspar and carbonate crystals, and the

Jong axes of amphibole prisms, may define S,.

A moderale quartz c-axis fabric has been noted

im some specimens of quartzofelspathic schist

and ay early quartz veinlet cutting the S,

surface of a quartz-felspar rich schist in the

north-west block was observed to be recrystal-

lised and to have uw strong quartz fabric in

which most c-axes were aligned within the S,

surtace,

A fait to strong mineral streaking lineation

is notable within the S, surfaces cof some

exposures. This lineation is defined by elongate

mica plates and porphyroblastic knots in

schists and by amphibole. prisms in calcareous

rocks. A set of cross joints is commonly scen

lo lic perpendicular to this lineation. In the

mica schists the lineation. is defined by a ¢om-

binalion of two cllects, Firstly the mica plates

are up to twi¢e as wide parallel to (001) in

the direction of the lineation than they are

across it, the biotite plates being considerably

more stumpy in form than assoctated musco-

vite plates. Secondly the mica plates 2re much

more diversely oricnted in sections cut per-

pendicular to the lineation than they are in

sections cut parallel to it: that is, the mica

plates are fautozonally arranged about the

lineation axis. In the absence of suitable strain

markers in the present arca it is not possible to

determine whether this lineation as due to the

mimetic growth of crystals in lines of bedding-

cleavage mtersection, L{S,-S;}, of is a tectome

strain lineation, L(S,), developed during meta-

morphic mineral growth, The penetrative

nature of this lineation in many cocks, and

strain shadow ejfects around syntectonic por-

phyroblasts, favours the latter.

No mesoscopic B(Sy+S,) folds have been

observed, In sone schists in the north-west

block o mild crenulation in the S$, surface,

showing syntectonic crystallisation of the mica

plates in the crenulation hinges, suggests

effects of the F, event. Some mesoscopic

F. folds of hand specimen size have been

found as Aoat in the north-west block, but they

are apparently quite rare. These folds show §,,

parallel to 8, folded into V-shaped sivles with

planar limbs, well defined hinge regions wad

thickened noses.

Likewise the effects of the Fy, event are

weakly developed in this sequence, The

PARK 3s

Gumeracha Goldfields antiform in the south-

east has macroscopically flexed the 8, and 8,

surfaces, but otherwise, only aecusional bax-

like post-crystalline c¢renulatians, showing

strong strain effects in the minerals of their

hinge regions, are considered to belong to the

F.. event.

Biatite zone

West of the Williamstown-Meadows fault

line fine-grained impure dolomites, dolomitic

phyllites, phyllites and phyllitic slates bhelong-

ing to the biotite zone are also characterised

by multiple defarmation, Evidence for ihree

overprinted deformation phases can be recog-

nised in some exposures and provisionally

equated wath the B,, Fy and Fy events. These

rocks have a very fine grain size, quartz and

micas averaging 0.01-0.015 mm, and invari-

ably have a strong §; slaty cleavage labric

defined by the shapes of curbonate grains and

the parallel orientation of muscovite and bio-

lite plates. "Strain shadows" are presence

around some opaque minerals, The ¢c-axes of

quurle grains possess a strong orientation in

the S, fabric of some phyllites, with most

c-uses tending to Te im the S, surface.

S; is seen to lie at large angles to S, in some

exposures and broad hinge regions of B(S,-5,)

folds are present. So is usually well defined by

compositional layering or Jaimination.

At 890120 well developed finely spaced

strain-slip or crenulation cleavage, Sy. was

observed in phyllite. Microlithons between the

crenulation cleavage planes. are about 0.3 mm

in width. The S, cleavage within the micro-

lithons as bent into the S, crenulation cleavage

surfaces and this process ts ackompanied by

unm increase i mica content within the Sy,

surfaces. Apparent displacement on the S, sur-

faces crossing the phyllite is not represented

as displacement in cross-cutting quartz vein+

lets, but as. sharp monoclinal folds with

atienuated limbs crossing the S. surface,

Where S, is developed, mesoscopic 8(S)-S.)

folds are observed in the bedding (Fig. 4h).

QQuartzose layers are buckle folded, while car-

bonate-rich laminated phyllite layers are strain

slipped. ‘The folds are disharmonic on all

ecales, but the So surtuces tend to have 4

consant orientation. Thin quartz stringers

were seen to have been ptygmatically folded

un a microsenpte scule in the Fy event. Later

more brittle Kink folds are rarely observed

and might be attributable to a weak Fy event.

FAULY SPRUCTURES

Thrust faults

Several thrust sheets have been mapped in

(he present area on the basis of metamorphic

and structural discontinuities. Vhese thrust

sheets Wert emplaced during or after the Fy

event and were subsequently folded in the F,

eveot. Four principal thrusts are named. The

Wirriynda “Uhrust, passing near “Wirrianda’

homestead situated on the southern shore of

the reservoir; the Watts Gully Thrust, passing

close to the site of the richest gold discoveries

in the Gumeracha Goldfields; the Sanctuary

Vhrust, largely confined to the flora and fauna

sanctuary in the south-west; and the Murray

Vale Vhrust, named after the pastoral property

south-east of the headquarters of the Mount

Crawtord Stule Forest. The Jast three named

faulis appear to be hinged near the southern

margin of the mupped area. The opalised

Iremolitic rock bed at the contact of the

mictasandstone and the course-grained schist

sequence has proved to be a useful marker

horizon in the identification of sequence repe-

tiliom in the thrust sheets, There are no proven

natural expasures of the thrust Fault surfaces

in the area, and critical thrust shyet interplay,

particularly in the south-west. ig obscured by

alluvium and poor ouicrop, There is some

evidence From the study of the mesascopic

orientation data that the higher sheets rotated

clockwise oVer the lower sheets in the south-

west corner of the area. This may be the

result of rotation during the thrusting move-

ments or differential rotation of the sheets in

the subsequent F, event. Numerous exposures

of sheared and mylonitic gneisses in the thick

pelitic seyuenve are thought Io have been deve-

loped during the thrusting movements,

On the northern slopes af the reservoir the

Wirrianda Thrust is marked by a sharp

contact between metasandstone and course-

grained micaceous eneisses. South of the

reservoir the sandstone cuts out and the hase-

ment gneisses are brought into contact with

the schists and gneisses of the Adelaitlean

sequence, Although exposure is fairly good

here. similaritics between rock types and the

overprinting of mesoscupic Fy folds From the

Adelaidean schists into the basement racks

have obscured the actual fault surface, Further

south the upper section of the metasandstone

\nit reappears. but the fault zone is everywhere

obscured by soil cover, North of Watts Gully

(he fault line follaws the bottom of a steep

Veshuped valley and its actual path across the

K. J, MILLS

mctasandstone further ta the south-west has

not been identified. but it is assuined to

eventually rin mto the Willramstowm-Meadows

Paull.

Structural evidence jin support of the Wutts

Gully ‘Thrust is obtained from an area of

woderate exposure near the centre of the

patch of virgin scrubland of the flora and

fauna reserve south-west of Dead Horse Gully,

Here considerable discordance exists between

structures on either side of the mapped fault

trace, and 4 narrow splinter of pebbly

micaccous mctasandstone appeurs ta lic

within the fault zone, The Watts Gully Thrust

is also responsible for a repetition of the strati-

graphic sequence, Near Watts Gully the fault

trace can be followed us 4 junction between

schists and metasandstone and js marked in

places by a distinctive white albite rich rock,

which may carry tale or actinolite crystals.

Under the microscope this rack is largely cam-

posed of well-crystallised untwinned plagioclase

with a composition near pure albite, carrying

occasional rutile inclusions, Some interstitial

quartz grains with slightly undulase extinction

are dispersed through the albite, Scattered

muscovite plates, preserving & microstructure

like that of Sy in the pelitic schists, ure

strongly bent and are encased or adjoined by

the unstrained post-tectonic albite.

The Sanctuary Thrust is of limited extent

and is defined on the basis of a repetition of

& belt of metasandstone shove pelitic schists,

The fault trace is also marked in a few places

by a peculiar white albilte rich rock similar

to that described above,

Movements on the Murray Vale Thrust

were of greater magnitude than those on the

underlying thrusts and resulted in the conjoin-

ing of racks of markedly differing metamorphic

and structural character, as described in

previous sections, Fxposures of rocks near

the thrust surface are very rare, and for

most of ils length the thrust line is marked

by a conspicuous strip of soil cover. In the

field the position of the thrust has been placed

on the basis of the readily mapped distinction

between the coarsely crystalline rocks of the

sillimaniteanuscovité zone and the medium cto

fine-grained schists of the andabusite-kyanite

zone. Much of the eastern margin of the

granite gneiss has been reinlerpreted as the

thrust surface. The banks of a road cutting

on the improved section of the mitin road

south of the reservoir, about half a kilometre

north of the headquarters of the Mt Crawford

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

Stale Forest, expose rocks on either sid¢ of the

Murray Vale Thrust, Fine-grained schists and

the thick opalised tremolite rock bed lit in

conjunction with weathered amphibohle wand

coarse-grained mica schists with intrusions. af

pegmatite, The faulted contact is marked by

& Narrow zone of green clay-like pug.

The Murray Vale fault linc has been super-

ficially traced north of the reservoir where it

is marked in a few places by a sugury while

albite rock containing green actinolilic spots.

After passing through a left-handed displace-

ment, probably a large F, fold, it traverses

the centre of the large quarry excavated for

clay und sillimanite. Near the base of the

quarry the fault zone is seen to be less than

half a metre in width and filled with pale

greenish clay-like pug. The fault surface dips

easterly at about 70° with some irregularities

caused by open Fy folds, On either side of

the faull extensive shearing, especially in the

higher grade rocks to the west, has resulied

in the formatiin of the unique Williamstown

damourite schists containing kyanite uni

corundum, massive sillimanite pods and clay

Uepusits. The clay Ueposits seem to be related

to Inte stage alleration within the faule zune.

Wesl of the fault ale a variety of high grade

poeises Showing Jess allteralion to clay away

from the fault surface. Fine-grained lower

grade schists are exposed cast of the fault.

Same are very fine-grained pyritic schists

which are extensively altered to clay near the

fault, although still preserving Hresh pyrite

cubes near the base of the quarry. Some open

fokis, presumably of the F,, event, are visible

in the lower grade rocks. North of the quarry

the Murray Yale Thrust probably passes

through another lurge F., fold resulting in the

uppearance of fine-grained quartz-felspar-

biotite schists displaying open shallow north-

phinging F, foldy in small quarrics north of

the forked junction of the rounds Jeading to

“Spritigheld"’ and the Australian Industrial

Minerals quarry.

The Ukeaparinga Fault

The Ukaparinga copper prospect in the

north-west corner of the area is situated

within the brecciated zone of a major meta-

morphic and structural discordance, herein

named the Ukaparinga Fault, Displacement on

this structure must be at least as great as thot

on the Murray Viele Thovist, but it is ancertain

as to whether this faull should be grouped

with the pre-Fy thrusts or i a brauch of the

nearby post-F, Williamstown-Meadows Fault,

which it joins a little south of the South Para

River, A fillle 19 the west of the Ukaputinga

Fault, # parallel fault line has been traced on

ihe grownd in an area of moderale exposure

of the sehisty of the kyunite-andalusite zone

sequence, but its importance as a fault struc:

lure has not been determined.

The Williamstawn-Meadows Fault

An important fault line, separating fine-

grained biotite zone rocks from coarse-grained

amphibulile fucies rocks, can be traced in a

north-south direction on the western side of

the area, In eurlier literature this fault his

been referced to as the Kitchener Fault, but

as it appears that this name is based on a

misconception, and since the author has been

able to follow the path of this fault as a con-

tinuous line from well north of Williamstown

to well south of Meadows, the name Williams-

town-Meadows Fault is preferred,

Within the present area the actual fault zone,

along most of its length, appears to be very

narrow and sbhurply defined, although some

exposures of tectonically emplaced foreign

biogks lying within the fault zone fave heen

shown on the map as fault melange. Where

the fault line crosses deeply incised valleys, a

sleep easterly dip of about 60-70" has been

estimated for the fault surface at several

points. ‘This would suggest that the fault is

of the steep reverse Lype, bul unlike the thrusts

described earlier, movement occurred after the

F, folding episade,

A uarrow zone of brecetated phyllite marks

the fault zone al ong exposure north of the

South Para River. South of the river fine-

grained dolomites are brought against the fault

surface im several places and close to the

fault these rocks have been recrystallised to

medium-grained white dolomilic marbles can-

taining large plates of muscovite and talc and

minor amounts of quartz and felspar grano-

blusis and an opaque accessory, The ¢equi-

granular hornfelsic texture and the partially

dissolved nature of twin relics within the

carbonates suggesis That these marbles were

uffected by some form of contact metamar-

phism, It seems that the higher grade hanging

wall block was still sufficiently warm during

and after the fault displacement to contact

metamorphose the impure dolomites near the

inmediate contact with the fault surface.

In the south-western corner of the Warren

National Park float and outcrop of felspathic

and micacedus schists and gneisses of foreipn

texiural appearance, opalised tremolitic

marbles and metasandstanes testify to the

presence of a mélange lens within the fault

zone A further lens containing peculiar mica-

tich schists defines the fault zone separating

metasandstones from dolomitic phyllites

almost half way between this locality and the

South Para River. The microstructural features

of the schist blacks within the fault zone can

be provisionally correlated with the 8), 5,

and S. structures of the area, The meta-

morphic wrade of these schists seems (o be

that of the upper greenschist or Jower amphi-

bolle Caciex, A small stauroliie crystal was

found in a specimen of bjotite-rich sehist.

Apart from some kinking and bending of mica

plates and quartz grains and the introduction

of thi stringers of potash felspar, the fault

movenjents appear to haye had little effect on

the structure of these schists, and the faulting

appears to have occurred when the metas-

morphic temperatures were too low to permit

any significant recrystallisation.

The amount of displacement on this fault

must be very large judging [rom the meta.

morphic diflerences between rocks on either

side of the fault surface. Miles (1950) suz-

gested a minimum displacement of 5,000 with

a probable displacement of ahout 10,000’, Dis-

placement of the order of 3 to 5 thousand

metres does not seen incongruous, but a better

estimate of the amount of displacement must

uwail a amore detailed study of the strati-

Braphic and metamorphic relationships along

mast of its length,

burlier workers (Miles 1950; Sprige 1945)

have considered the possibility of Tertiary to

Recent movements on this fault, the evidence

for this being based on the marked fault scarp

expression and the occurrence of erosional

surfaves and gravel beds of supposed Tertiary

uge west of the fault line near Williamstown.

However, hills composed of Adelaidean bed-

fack in the south-west of the present area are

al the samme height on either side of the fault

line, and there is no evidence of recéni re-

juvenation on the fault surface. The fault

acirp i$ believed to be due to the erosive

power of the Soath Para River and its tibu-

tariey removing the more readily disintegrated

biotite zane: phyllites and dolomites west of

the tault, after crossing the resistant Warren

Infier and iis mantle of metasandstones and

schists. This erusional scarp was probibly in

existence during the formation of the Tertiary

KF MINS

gravels and lateritic surfaces near Williams-

town, with the Warren Inher and its swirround-

ing mantles of high-grade rocks protruding

above the Tertizry erosion levels,

CoONELUSIONS

(£1) Basement-Adeluldean relationships

Howchin (1906, 1924) clearly recognised

the existence of basement rocks in the porge

of the South Para River, south of Williams-

lown, and claimed that an unconformity

separated the basement from the underlying

metasandstones of Aldgate Sandstone type,

Hossfeld (1935) claimed to have recognised

an actual exposure of the unconformity near

the Warren Reseryoir weir, but this could not

be confirmed in the present study, Luter

workers (Campana 1953: Mills 1963) tailed

to recognise a basement inlicr. Campana

apparently regarded the lowest schists a5 metu-

somatic alteration products of the Aldgate

Sandstone equivalent and Mills interpreted the

schists below the metasandstone as an early

Adclaidean pelitic sequence, The present study

hus confirmed Howvhin’s claim for the

exisfence oF a basement inlier, Marked struc-

tural discontinuity across the observed uncon-

formity surface discounts the possibility of an

early Adelaidean pelitic sequence. The cosrse-

grained schists and gneisses above the mceta-

sandstone unit Jithologically resemble the

basement yneuses, but they contain mesuscupic

structures which may be correlated with unu-

logous. structures. in the metasandstone unit

and not with structures in the basement

gneisses.

Io the nearby well-established Houghton

Inlier, Spry (1951) showed thal schistosities in

the basement and in the Adelaidean mantle

were generally parallel. ‘The schistosity in the

basement was interpreted as a retrograde

schistosity which was associated with the

Pulteozvic folding of the Adcluidean succes-

sion and updoming of the basement, although

tere was some evidence (Spry 1951, p. 120)

for shearing of the basement prior to Ade«

dsidean sedimentation, Campana (1955) sug-

gested that movements in ihe basement of the

Adelaide region were responsible for the

folding of the Adelawewn sedimentary mantle.

the lower beds of which were consequently

adjusted into tight folls characterised by

sharply overturned anticlines, with attenuated

limbs grading into overthrusis and broad

¢ortugated synclings, Talbot (1962) curried out

an extensive study of the southern part of

SIRUCTURAL CEOLOGY OF WARREN NATIONAL PARK 49

Fig, ¥,

Hee alts

fa a if shee)

Block diagram constricted to scale in orthographic projection on a line of sight plunging 35°

towards 253° showing the forms of the principal stractural surfaces in the vicinity of the Warren

Reservoir, The structural surfaces shown are the thrusts and faults (cross-hatched), unconformity

-etween the basement rocks of the Warren Inlier and the Adelaidean sequence and the lop

of the Aldgare Sandstone equivalent (stippled). The surface of the block corresponds to the

high water level in the Watren Reservoir but detailed adjustment to the map pattern to allow

For topographic variitions have not been made, The F, synform outlined by the unconformity

in the centre of the diagram is overprinied by macroscopic be folds, and other Fu folds are seen

near the Warren Reservyir, The structural surfaces are folded by larze Fs folds in the southern

part of the diagram «nd lesser Fz folds are interpreted to deform the Murray Vale Throst: lo

the north of the reservoir.

the Houghton Inlier and its Adelaidean mantle

abd considered that the chlorite grade base-

ment “acted a5 a simple core structure and

adjusted to the folding of the overlying

Torrens Group" by passive movement along

foliation planes produced in a pre-Adclaidean

Tetrogressive phase.

The present study has established that the

lower portion of the Adelaidean succession

is welded onta the basement rocks of the

Warten Iplier ond that the basement rocks

were rejuvenated during the deformation

events and the extensive metamorphic recrys-

failisation which affected the overlying Ade-

laidean sediments during the lower Palacovoic

Delaincrian ofogeny. The surface of uncon-

formily has been infolded into the basement

encisses and there is little evidence of any

differential mayement at the boundary between

the basement rocks and the overlying sedi-

mentury mantle. The basement rocks of the

Warren Inlier have undergone 4 partial tee-

tonic reconstitution ji which the lower

Palaeozoic folds wens imposed on the older

pre-Adelaidean structures.

(2) Folding of the Adelaidean succession

Regional studies in the Mt. Lofty-Olary

orogenic arc have indicated that the upper

Proterozoic (Adeluidean) and lower Palaeozoic

successions were affected by only a lew gentle

epeirogenic episodes (Sturtian tectonisin, Dut-

tonian folding, Cuassiniaw and Wailpingan

movements) prior lo a major orogenic revolu-

tion. (the Delamerian Orogeny) in lower Ordo-

vician time (Thomson, in Parkin 1969), This

ofogenic cycle brought about cxtensive fold

deformation, created a helt of low to: inter

mediate pressure metamorphism and’ granite

intrusion, and brought an end to geosynctinal

sedimentation in the Mt. Lofty Range region.

The syntectonic Palmer granite, intruded into

the core of the metamorphic belt in the eastern

Mt. Lofty Ranges, bas been isotopically dated

at 490 million years (White, Compston &

Kiceman 1967).

Detailed structural studies in several key

areas in the Mi, Lofty Ranges has established

that three important episodes of fold deforma-

tion look place at various stages during the

‘ia K. J, MULLS

metamorphism, Oller & Fleming (1968) syn-

thesized previously published and unpublished

work relating to the deformational and meta-

rourphic history of the Mf, Lofty Ranges and

ussumed that euch of the three folding

episodes (F\, Fa and F,) were synchronously

developed across the whole deformed belt, but

it seems that more key areas will need to be

unulysed before this premise can be verified

and a satisfactory unravelling of the deforma-

tional history is achieved.

The present structural study of the upper

Prolerozoic rocks around the Warren Inlier

has established that three distinct tectonic

episodes myolving fold deformation have

occurred in succession in relation to meta-

morphic recrystallisation,

F, deformation

Bedding surfaces (Sy) of the Adelaidean

succession Were deformed into large regional

folds during recrystallisation of the sediments

under conditions of rising metamorphic tem-

peratures and mica plates and other meta-

morphic minefals. grown or deformed syntec-

tonicully, developed 9 strong axial surface

schistosity fabric (S,) containing an inter-

related axis of elongation, 1{S,), which is

expressed aS a minecal streaking lineation in

some exposures. The commonly observed near

parallelism of S, and S, suggests that these

early folds possessed an isoclinal style with

extensive oear planar limb areas. Mesoscopic

F, folds ate apparently rare and difficult to

identity, and litthe can be deduced Irom the

initial geometry of the F, deformation within

the vonfines of the small area studied. Struc-

tural analysis of the bedding attitudes in the

basul iietasandstone suggested that the hinwe

lincs of macroscopic F, folds were gently

plunging or subhorizontal and it can be

assumed from regional studies elsewhere in the

ranwes that the hinge surfaces of the F, folds

were dipping stccply cast and striking north-

south purullel tu the tread of the orogenic belt

(Offler & Fleming 1968), The regional struc-

ture which Campana ¢? af. (1955) named The

(Lookout Tower overturned anticline can be

considered to refer io the demal structure

comprising the culmination of the Warren

Inlicr, although this culminution is the cam-

bined resultant of the Fy, Fy, and F, folding

events,

‘Textural-mincralogical evidence sugecsts that

metamorphic lemperateres hid reached a peak

by the emf of the F, deformation, or during

the interkinematic period between Lhe Fy and

F, events and the marked metamorphic zona-

tion observed in this area Was impressed al this

time. In the higher grade schists the mica and

quartz grains defining the plane-linear S)-L( $1)

labric had developed a coarse praili-size and

sillimanite fibres and prisms had grown within

the $, surfaces prior to the commencement of

the Fo deformation. Despite high-grade mets-

morphism sedimentary clasts and textures are

slill preserved in must specimens. of the coarser

arenites, even in specimens exhibiting @ sirong

S,-L(8,) fabric. In those metasediments

assumed from their composition to have in-

iiated as pelites and semi-peliies recrystallisa-

tion and grain growth has obliterated all signs

of sedimentary structures in the coarser

grained rocks of the sillimanne-muscovile

zane, but thin bedding laminations are pre-

served in the finer grained schists of she

kyanite-andalusite and biotite zones,

F, deformation

This dclormation episode commenced at or

near the peak of metamorphic tenyperature,

allowing recryslallisalion and grain growth

processex to become dominant over strain

preservation in some rocks, and allowing the

F, strain effects to outlest grain growth in

others. The resus of ihe F; deformation are

expressed in two principal forms:

(1) The development of intensely appressed

folds in the earlier Sy and 5S, surfaces and the

imposition of a strong crenulation cleavage-

schistosily (Sy) with a north-south strike ane

a steep easterly dip, and

(2) the development of major late-meta-

morphic thrusts which now divide the area up

infe several distinct stryotural-metamorphic

fumes.

The penctrative effects of the F., deforma-

lion are most pronounced in the coarse micu-

rich schists and gneisses of the sillimanite-

muscovite zone where intensely deformed isu-

clinal folds in lithological layering have 32

well-developed crenulation cleavage (So}

(crenulation of the S, schistosity) grading into

a new coarse-grained schistosity as yn axial

surface structure. In many exposures the Sy

schislosity has become the dominant penetra-

tive structure and traces of the former §,

schistosity are preserved only in the form of

a strong mineral streaking Jineation L(S,-So).

The Mount Crawford pranite gneiss formed

during the F. deformation and presetves a

well-developed S. schistosity and a constantly

oriented mineral lineation interpreted as the

STRUCTURAL GEOLOGY OF WARREN NATIONAL

L(S,-S.) intersection lineation, Basic dykes,

intruded helore or during the F, event. re-

crystallised to schistose amphibolites preserving

a strong amphibole prism lineation, which is

interpreted as the result of mimetic growth of

hornblende prisms parallel to the .(S,-Sol

intersection lineation,

The effects of the F. deformation are Jess

pronounced in the mutasandsiones. and,

although F, crenulations are well developed m

the more mica-rich Varieties, intergranular

movements were probably daminant, Meso-

scopic F, folds in the metasandstones show

strong appression und Hattcning of the quariz

grains info the S, surface. In some ufcus some

of the plastic strain induced im the areniles

during the F, deformation outlasted recrys-

tallisation and strain relief. leading to the

developrnent of well-orientated quartz c-axis

fabrics.

In the lower grade kyanite-andalusite and

biotite zone blocks the FP. deformation is aot

50 apparent and the S». crenulation cleavage

is only locally evident, although some local Fy

mesoscopic folds are to be found and show

a similar tight uppreasion.

The Fy, deformation culminated in the ap-

pearance of several steep thrusts and mylo-

nilic zones iwvolving considerable, but as yet

unknown, amounts of displacement,

Following the Fy deformation, a sceond

static interkinematic period is envisaged in

which the strain preservation fromm the Fs

deformation became relieved under greenschist

fucivs conditions resulting m the exilensrve

retrouression of higher grade minerals to

quartz, albite, chlorite, sericite and rutile, The

sercite has undergone patchy regrowth to

larger randomly oriented muscovite crystals,

The growth fabrics of these late stage minerals

tend to be isotropic except where they were

mimetrically controlled.

Fy deformtation

Most parts of the area covered in the

preseril survey were affected hy a rather more

brittle deformation late in the metamorphic

Nistory resulting in smucrescopic and meso-

scopic. folds in earlier structural surfaces. The

Fk, deformulion is more pronounced in certain

zones. F, folds are rounded te angular and

PAKK 311

show varying degrecs of appression. ranging

From open warps with eust-west hinge surface

trends to tight folds with north-south hinge

surface trends and a weakly developed crenus

Jation cleavage (S,). Both the hinge surfaces

and the hinge lines show considerable varia-

tion in attitude, Minerals grown dunng the

earlier relrogressive metamorphism became

deformed during F, folding and show signs

of both plastic and brittle strain. The preserva-

tion of such fime F, strain features as quartz

deformation lamellae suggests What very little

erystal recovery took place after the F, event.

The fold deformational history outlined

above is in general accord with the conclu-

sions of other structural studies carried out in

the Mt. Lofty Ranges (Offler & Fleming

1968). At this stage it seems valid to correlate

the present results wilh those from the Pewsey

Vale area 10 km north-east of the Warren

Reservoir where Offler (1966)! found three

deformational events in the Adelaidean sue-

cession which appear analogous to those

described here. In the Pewsey Vale area F,

tolds were rare and S, was almost parallel

to Sy, some mesoscopic F., folds were deve-

loped and open macroscopic Py felds dami-

nated the regional structure. Metamorphism

had reached its peak late in F; or during F,

and was waning during the FP, event, Strong

crossed girdle quartz c-axis patterns developed

within quartzites after the F, phase but priot

to the Fy event. In the adjacent Kanmantoo

Group sediments at Pewsey Vale, Offler re-

corded two deformational cvents which he

interpreted as F, und Fy, with metamorphism

oullasting the F, event, In the Cambrai-Spring-

ton region Mills (1964)° found that the Kan-

mantoo Group metasediments were tightly

folded in a dominant early deformational

event with focal over'priating by a second fold

event with the metamorphic peak being

reathed during and folluwing the second

event,

(3) Faulting

Two varieties of faults have been distil

guished in the present survey), firstly, faults

and mylonile zones considered to be of a high

angle thrust type, which developed late in the

F, deformational event and wert subsequently

folded in the F. event: secondly. a high angle

* Offer, R, (1%66)—The stenctuve and metamorphism of (he Pewsey Vale atea, north-east of Williams-

_ town, Soulh Ausiralia. Univ. Adelaide, Ph.D. Thesis. :

* Mills. K. J. (1964)—The sirucrural petrology of au area east of Springton, Sout Australia, Univ

Adelaide. Ph.D. Thesis.

312

reverse fault, the Williamstown-Mcadows

fault, which developed after the Fy event and

has a tegional significance within the orogenic

belt.

The late Fy thrusts developed soon alter

the pewk metamorphic temperatuses had been

treuched and movements continucd during

waning Iumperatures. Some strongly schistese

retrograde rocks have formed within the thrust

zones, including the interesting Williamstown

danvourile-kyanite-corundum schists, Dis-

Placements on some of these fhiwsts were

large, and in the case of the Murray Vale

thrust, blocks with considerably different struc-

tural and metamorphic character have been

brouphe into conjunction.

Thrust faults (strike faults, overthrusts) have

beeo described from various parts of the Met.

Lolty Ranges, but us yet few have been ade-

Yitately mapped. Howchin (1906) recognised

an vyerthrust helt in the foothills of the Mt.

Lofiy Ranges near Adelaide and envisaged an

cast lo west movement. Sprigg (1946)

desenbed this belt in greater detail and con-

cluded that the amount of over-tiding was

small. Thrusts und strike faults are also well

established on the western side of the

Houghton Inlicc (Benson 1909, p. 105; Spry

(951; Campana ef a/, 1955). Freytag ( 1957)"

recoynised and mapped several strike faults

north of Williamstown and his Enterprise

Fault may eventually prove to be a continuar

ton ef the Murray Vale Thrust of the present

survey,

A portion al the Wilhamstown-Meudows

Fault has been closely mapped in the present

survey. I'he outcrop trace o/ the fault surface

provides evidence of a stcep easterly dip and

the fault may be classed as a steep reverse

type (see also Thomson, jn Parkin 1969.

p. 108), The actual displacement directions and

the amounts of displacement are unknown,

but a dip-slip component of 3+5,000 metres

dues nop seem incongruous with the observed

metamorphic grade differences across. this por-

tion of the fault surface. Recrystallisation of

dolomitic marbles in the lower grade block

aujacenr to the Cuult surface suggests heat

derived from fault movement or from a still

warm uplifted higher grade eastern block,

Erratic schistose blocks carried within the

fault zone carry a metamorphic mineral assem-

blagé suggestive of lower amphibolite facies

K. J. MILLS

conditions. It is sugested that movement! on

this fault occurred during waning metamor-

phism in lower Palaeozoic time, There is no

evidence of any more recent rejuvenation of

movement on this fault and the present fault

scarp is 4 geomorphological erosional feature,

Further investigation will be necessary to

establish whether the economically important

Ukaparinga Fault is a branch of the Williams-

town-Meadows Fault or & steep thrust of the

post-F. type,

(4) Willianistown Window

A great deal of confusion seems to have

arisen in the previous literature regarding the

interpretation and significance of the coarse

grained schists ond gneisses in the Williains-

town-Warren Reservoir region. These rocks

were initially regarded us basement rocks by

Howchin (1906, 1926), bur Later workers (e.g.

Alderman 1942, Campana 1953, Campana

ev al, 1955) considered them to be of meta-

somatic origin. Campana (1953) mapped them

as the “Aluminous metasomati¢ zone of South

Warren Reservoir’ on the Gawler 1-mile

Geological Sheet.

The present study has establixhed that these

Bieisses are in part basement gneisses of the

Warren Inlier and in patt metamorphic

equivalents of the ower portion of the Ade-

laidcan succession. The present author inclines

to the view that the schists ancé gneisses may

be the result of an isochemical reconstitution

of initially alminous pelites of mot unusual

composition under high grade metamorphic

conditions within the — sillimanite-muscovile

zone of the amphibolite facies. Vheir striking

texture pnd coarse grain-size is a result of

syntectonic crystallisation mear the peak tem-

perature of metamorphism within a zone of

lacally intense [5 deformation. Adjacent meta-

sandstones, although showing remarkably well-

preserved cross-bedding, and cyen some clastic

grain textures, huve, in fact. been subjected tes

similar metamorphic conditions. Later Fs up-

thrusting of the Warren Inlier und ifs sur-

rounding mantle of high grade Adclaidean

metasediments, principally on the Murray Vale

Thrust, and later updoming in the Fj phase

and subsequent erosion has exposed a unique

kind of tectonic windew within which we can

examine the metamorphic and structural re-

constitution of the pre-Adelaidean hasement

" Freytag, FB ('947)—The Vietoria Creek Marble, with observations of the geology of an area north-

east Of Williamstown, South Australia, Unt. Adelaide. Honours B.Sc, 'T

hesis.

STRUCTURAL GEOLOGY OF WARREN NATIONAL PARK

and the lower levels of the Adelaidean suc-

cession in the core of the orogenic belt,

fe is proposed to call this structure the

Williamstown Window. Rock units within the

window comprise the basement of the Warren

Inlier, the basal metasandstones in the Wil-

liamstown region, and the overlying coarse-

grained Adefaidean schists and onersses

belonging to Campana’s "Aluminous meta-

samatic zene of South Warren Reservoir”,

(5) Economie Considerations

li seems apposite to present here a few

comments on the structural conirul of same

af the economic mineral concentrations within

the area surveyed.

The Ukaparinga (Unapannga) Copper

Mine, Jocated in the north-west corner of the

mapped area, was worked in 1350 as the

Wheal Fricndship Mine (Brown 1908, p, 137:

Cornelius 1940) although apparently littl ore

was won. Thete hus been some renewed in-

terest in this deposit as 4 low-grade copper

prospect in recent years (Blissett 1965). This

deposi is located within the Ukaparingu Faull

zone which has been traced south of the mime

property, From Blissett’s description of the

mineralized zone within the mine the fault

zone would appear to be dipping 65-70° east,

and this fault is a steep reverse type with a

very large component of displacenvent, A

point uf some interest is that the thick tremo-

litic marble bed mapped in the South Para

yorge, suuth of the mine, can be predicted to

occur within the footwall block bencath the

mine, and this might portend a more richly

mineralized zone at depth. Tt is not yet knowa

whether the Ukaparinga Fault is a branch of

the Williamstown-Meadows Fault or is a late

F.. thrust fault. Several other copper prospects

are located within sinnlar fault zones north of

Williamstown.

The short-lived Gumeracha and Muunt

Crawford Goldfields, located uround Watts

Gully in the Mount Crawlord State Forest,

were discovered in 1884 and developed as an

alluvial field. Numerous shafts were sunk in

an attempt to locate the source of the gold,

hut the gold was apparently confined ta quartz

leaders of small size which proved utpayable

(Brown & Woodward 1886), The known gold

distribution in this field is confined to the hinge

region of a large F, antiform, the Gumeracha

Goldficlds Antiform, and it scems likely that

the auriferous quarts leaders were loculised

wilting (ractires associaled with this brittle

Jute metamorphic fold structure. This struc-

J|3

tural control may prove to be of some interest

in the interpretation ol the distribiillon of

other goldfields im the Mt, Lo'ty Ranges,

The Williamstown clay deposits have been

worked in the vicinity of the Warren Reservoir

since early this century, Several older disused

mines are located south of the reservoir within

the mapped area, especially within north-south

zones of highly altered rocks running immedi-

alely east of the Wirrianda homestead and east

of the road immediately south of the old road

bridge, buf the main quarry currently operated

is that in section 950, Hundred of Barossa,

just outside the north-cast edge of the mapped

area. Many reports have been wrillen On these

deposits but hitherto no important structural

control has been recognised. Jack (L926) sug-

gested that the kasolinisation and hydromica

development was preater than would be

expected by weathering alone and suggested

some Form of introduction. Cornelius (1932)

indicated that the deposit in section 950

dipped steeply east and had a southerly pitch.

Alderman (1942, 1950) concluded that the

cluy deposits had largely originated through

the hydration of an original body of massive

decussately textured sillimamite rock and

erected an elaborate metasomatic scheme to

explain the various phases present and the

sudden changes from low grade to high grade

rocks. Alderman (1942, p. 8) states that “there

dovs not scum to be any major structural

feature separating the aluminous rocks Irom

the low grade rocks”, Later workers (Gaskin

& Sampson 1951, p. 60; Betheras 1953;

Cochrane 1954, p. 54: Cochrane 1955, ». $5)

generally accepted Alderman’s views, and

although there are references fo various

damourite shears and small faults, these are

cunsidered to be of minor importance. and

perhaps cue to volume changes during metu-

somatism, The clay deposits appear to be

irregular in distribution and this was related

fo the fortuitousness of metasomatism.

The clay deposits north of the reservoir

were not studicd by the author, but pre-

liminary observations have tndicaled that the

Murray Vale Thrust passes through the centre

of the large quarry on section 950 and

separates the highly altered sillimanite-kyaqite

bearing rocks to the west front the low-grade

“clay-states" to the east. It the vicinity of

the quarry the Murray Vale Thrust is ap-

parently involved in Several tight F, folds,

Tn terms of the structural history deter-

mined for the schists occurring south of the

js K, J. MILLS

reservoir, the following series of events is

envisaged us controjling (actors in the forma-

tion of the clay deposits, The original mussive

sillimanite-rutile rocks are thought to have

crystallised within the sillimanile-nmiuscovite

zone schists and gneisses at the peak of metu-

morphism under static conditions during the

interkinematic period between the F, and F,

deformation events, The origin of the silli-

manite remains obscure, but presumably same

form of melasomatic transfer was involved.

During the Fy, event, whilst the country rocks

were being intensely deformed and reconsti-

tuted. a number of damourite-kyaniles. corun-

dum shear zones developed within the tectonic-

ally resistant sillimanite pods and late in the

F, event several strong thrust zones appeared,

and the subsequent passage of hot aqueous

solutions within the thrust zones altered the

sillimanite deposits to clay. It is considered

that the sillimanite and damonrite-kyanite

deposits may be structurally controlled within

early incipient zones of [F. Uhrusting, but this

will need further investigation. The subsequent

development of clay within some of the silli-

manite bodies may have required the presence

of open channelways along zones of tuter

movernent and could be enhanced by the deve-

lopment of strong Fy folds in the vicinity of

section 950,

(6} Sanpnary

The following list of events summarises the

proposed geological histary for the Warren

Reservoir region:—

{a) Deposition of pre-Adelaidean sediments

of the Warren Inlier. These sediments were

largely pelitic and homogeneous with some

quartzofelspathic units and minor mars.

(b) Deformation of the pre-Adclaidcan sedi-

ments of the Warren Unlier. Several phases of

folding, as yet unravelled, accompanied this

deformation, with metamorphism (o upper

greenschist or lower amphibolite facies at

most, There gre no intrusive tocks, apart from

pegmatices. no volcanics, no rocks of

“Houghton diorite” type, and no evidence for

a phase of pre-Adelaidean retrogression and

phylonitisation,

(d) Deposition of the Adelaidean sequence,

consisting of a basal cross-beddled felspathic

sandstone followed by a pelitic sequence grad-

ing upwards into more calcareous or dolo-

mitic sequences.

Adelaidean succession in the lower Ordovician

Delamerian orogeny. Three compressive events

accompanied this orageny and metamorphism

locally reached the sillimasite-muscovile zone

of the amphibolite facies within and adjacent

to the Warreb Inlier A locally important

phase of thrusting from the east accompanied

and followed the second compressive event

under conditions of waning metamorphic tem-

peratures. The third compressive event, ol

more brittle character, occurred during low

metamorphic lemperutures and played an im-

portant role in the development of various

mineral deposits,

(1) Formation of the Wilhamstown-

Meadows Fault as a major plane of discon-

linuily extending along most of the length of

the central Mount Lofty Ranges. ‘This fault ts

responsible for bringing the higher grade meta-

morphic zones of the eastern Mount Lolly

Ranges into conjunction with the lower grade

zones of the western Muunt Lofty Ranges.

Displacement on this fault occurred in the

early Palacozoic and there is no evidence of

subsequent rejuvenation of movements.

(zg) Extensive denudation and peneplanation

and development of a marked fault scarp ero-

sional feature along the Williamstown.

Meadows Fault in the Williamstown region

through the differential erosion of (he lower

grade phyllites by the South Para River.

Acknowledgements

The author is grateful for the co-aperation

of the various public autboritics and private

individuals who have permitied access to pro-

perty fo make this study possible, The project

Was completed in the Department of Geology

and Geophysics, University of Sydney. Mr. R-

Sealy kindly axsisled with photographic work

associated with the construction of the figures.

Mrs. J, Neilsen as especially thanked for her

patient redrafting of figure t. Mr, Glenn

Kulson yssistel with the lettering on figure 2

and the map legends, Mrs. R. McKenzic

typed the final manuscript. The venerous sup-

port of the University of Sydney in enabling

the completion of this work is gratefully

acknowledged.

References

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BENSON, W. N. (1909).—Petrographical notes on

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BETHERAS, F. N. (1953) —Clay deposit—Williams-

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Burssett, A. H. (1965),—The Ukaparinga (or

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CAMPANA, B., GLAESSNER, M. F., & WHITTLE,

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CocuraNne, G. W. (1954).—Warren refractory

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OBITUARY: THEODORE GEORGE BENTLEY OSBORN,

D.SC., M.A., F.L.S.

Summary

THEODORE GEORGE BENTLEY OSBORN

D.SC., M.A., F.L.S,

OBITUARY

THEODORE GEORGE BENTLEY OSBORN, D.Sc., M.A,, F.L.S.

2.x.1887 -3.vi.1973

Theodore George Bentley Osborn was born

in England and educated at Burnley Grammar

School and the University of Manchester. He

spent just over half of a long and energetic life

in Avstralia, occupying Chairs of Botany at

Adelaide and Sydney Universities and later the

Sherardian Chair at Oxford University, On

retirement he chose to return to Adelaide.

Osborn's research during the period 190#-

1912 was on the fungi, when he was u lecturer

in Economic Botany in the University of Man-

chester, In 1911 he was awarded the M.Se.

degree, and in 1920 the D.Sc. degree, from the

same University.

In 1912, Oshoen was invited to become Pro-

fessor of Botany, Vegetable Pathology and

Parasitology in the University of Adelaide,

eombined with the office of Consulting Botanist

to the Government of South Australia, and his

publications over the next nine years strongly

reflect the nature of this appointment,

Shortly before coming tu Australia, he mar-

ned Edith Muy Kershaw, M,Sc-., Assistant Lec-

turer in Botany in the University of Manches-

ter. They had three sons, Peter, Andrew, and

Richard, all of whom served in World War IT;

Andrew, an R.A.F, pilot, was killed in action

in 1942,

When he established the Department of

Botany in Adelaide in 1912, Osborn was only

25 years old and youthful in appearance, He

was fond of the story of how he went into the

examination hall, which was being supervised

by a middle-aged woman who had not met him,

and asked for the Botany I paper. She brought

him the paper and when he said “and while 'm

here [It have a look at the Agricultural Botany

paper too" she replied, “You'll do nothing of

the sort, young man, you'll just sit down there

and get on with your Botany I.”

Osborn developed the first degree courses in

Botany at Adelaide University, though Botany

courses had been given earlier under Professor

Ralph Tate. He took most of the teaching until

1916 when a demonstrator was appointed, fol-

lowed in 1922 by a lecturer in Plant Pathology.

The latter appointment, and the establishment

of the Waite Agricultural Research Institute in

1925, relieved Oshorn from much of his time-

consuming advisory work. However, in 1926

he was asked by the executive of the recently

formed Commonwealth Council for Scientific

and Industrial Research to review botanical

work in progress in Ausiralia, and further to

report on plant problems in Australia. In. 1927

he was appointed adviser to the Council and

was offered the dircctorship of their Division

of Plant Industry. However, at about this time

he applicd for the Chair of Botany at the Uni-

versity of Sydney, lo which he was appointed

in 1928.

During the early years of his residence in

Adelaide, Osborn deVeloped interests in plant

ecology, studying areas near Adelaide as well

as distant ones, stich as Franklin Island and the

Pearson Islands, off the west coast of Eyre

Peninsula. During a visit by Professor R. S.

Adamson (University of Cape Town), joint

studies were made of the ecalogy of the Ooldea

district and of Eucalypries Forests of the Mount

Lofty Ranges. ‘These. studies: were published in

the Transactions of the Royal Society of South

Australia. Osborn also published on two primi-

tive lycopods, (Isoetes and Phylloglosswn),

found for the first time in South Australia.

These ecological studies led to Osborn's great

interest in the vast arid region of South Aus-

tralia. He made numerous visits to the saltbush

areas and developed cordial relationships with

pastoralists. This culminated in the generous

gift of Messrs. Hamilton, Wilcox Ltd., in 1925,

of the Koonamore Vegetation Reserve, which

is now the oldest biological station, with con-

tinuous records, in Austrolia, The reset've,

‘Trans, HM, Soc. S. Aust, Vol 97, Part 4, 30 November, 1973

318

located 385 km NNE of Adelaide, was re-

named the “T, G, B. Osborn Vegetation

Reserve at Koonamare” i) |972. The first

important work on grazing and regeneration of

natural Vegetation its chese arid regians resulted

from the collaborative work of Osborn and his

two colleagues. J. G. Wood and T. B- Paltridge.

The reserve and nearby areas are still used

extensively by stall and students of the Ade-

laide Botany Department.

in 1928 Osborn became Professor of Botany

at the University of Sydney and he set about

rvorganising the undergraduate courses there.

He took the first year lectures and those in

plant physiology, as well as in ecology. At first

he continued to clear wp his ared zone research,

relaining direction of the Koonamure work

uotil 193), but increasingly he became in-

terested in the vegetation of coastal New South

Wales, In [930 he gave the Livingstone Lee-

Iures enuiled “Plaot Life in the Sydney Dis-

trict", with an ecological upproach. He was

interested in the xerophytic propertics of the

plants characteristic of this relatively high Tain-

fall area. In 1932, his Presidential Address to

the Linnean Socicty of New South Wales. was

on “The Plant i Relation to Water’, with spe-

cial reference to the properties of xerophytes

in being able to withsiand drought. Later, O3-

horns work itt ecology stimulated the interest

of his students in descriptive ecological

accounts of other parts of New South Wales,

including one on the ecology of the Myall

Lakes vegetation, jointly with R. N, Roherlson.

During his time in Australia, Osborn was an

aclive member of 4cientific societies. He was

4 stroug supporter of the Royal Society of

South Australia, contrihuting several papers

uml berng a Fellow since 1913 and Honorary

Fellow since 1955. He was a Council Member

1915-20, 1922-24, Vice-President 1924-25,

1926-27, anu President 1925-26. He played an

active part in the establishment of Flinders

Chase on Kungaroo Island, being a member of

the board from 1919 to 1927, and Honorury

Secretary and Treasurer 1921-25. Oshom was

alsa a member of the Linnean Society of New

South Wales from 1928 and President in 1932,

and President of Section M (Botany) of

A.N.Z.A.AS. in 1928, and a Vice-President

from 1924-25, The Royal Society of New

South Wales awarded him the Clarke Medal in

1958.

Osborn became Sherardian Professor of

Holany aid a Fellow of Magdalen College, Ox-

ford, in 1937, The Oxford Department was

very poorly housed in cramped surroundings in

an antiquated building in the Oxford Botanic

Giarden. This Bolanic Garden, founded in

1621, had been somewhat neglected. but Os-

born stinvulated collaborative work with the

Garden, which continued strongly after the

Department moved into the new laboratories

planned by him and consteucted shortly before

his retirement in 1953.

Oshorn's achievements ut Oxford have been

summarised in his obituary in TRe Tintes for

6 June 1973~—-There can be nu doubt that

under him the study of botany m Oxford

achieved an eminence which it had not before

reached even under more famous Sherarlian

Professors. Not only was the production of

original work in botany greater in quantily and

quality than ever before but of the undergra-

duates, demonstrators and research men pre-

sent in Oxford during his tenure of the chair,

eleven of more are or have been Professors

and heads of departments, and several mure

Readers in biological departments of Univer-

sitics in Britain and clsew here.”

In 1953, Osborn retired from the Chair at

Oxford sad returned to Australia, After a

period of residence in Adelaide, in 1957 the

Osborns moved to Melbourne where Mrs. Os-

born dicd a year later. Following this, Osbora

returned to Adelaide to live. During 1959 he

was Acting Master of St, Mark's College, of

which he had been one of the founders in the

carly 1920's, In 1962, when the Botany Depart-

ment celebrated its 50th anniversary, he was

appointed Professor Emeritus of the University

of Adelaide, having been given a similar title

at Oxford University on his retirement in 1953,

Osborn left Oxford well known, among other

things, for his course on Gyminosperms, ane in

Adelaide he was invited by Penfessor J. G.

Wood to give 4 course oo this group of plants

to third year students. This he contrnusd to do

for five or six years, and in 1960 published his

last paper, on the embryology and life history

of Podevarpus faleatus. Osborn had long in-

tended writing a book on the Gymnosperms,

but unfortunately this never came to fruition

Osborn made his home at St. Mark's College

during 1959, where he was associated with the

very capable seerctary Marjoric Sabine, whom

he married in England in 1960. Both Professor

and Mrs, Osborn took an active part in the life

of the Botany Department from then on, and

Osborn attended the weckly seminars until

shortly before his death,

Oshorn was a good lecturer and teacher who

attyacted students of quality, His influence was

passed on toa several of the present leaders in

Australian plant ecology, and among his many

Australian students were: J. G, Wood (for-

merly Professor of Botany, Usmversity of Ade

lade}, Ci. Samuel (formerly Deputy Chiel

Szientific Officer of the Agricultural Research

Council, WK), G. J. Rodger (formerly

Direztor-General of Forestry, Canberra), B, H.

Bednall (formerly Conservator of Forests,

South Australia), T. B. Paltridge (formerly

Chief Scientific Liaison Officer, C.S.1.R,0,),

N. A. Burges (formerly Professor of Botany,

University of Sydney, and Vice-Chancellor,

University of Northern Irclandi, M.R. Jacobs

(formerly Director-General of Forestry, Can-

berra). D. Martin (Officer-in-Charge, Tis-

mangn Regional Laboratory, C.S.1R.O.),

H. K. C. Mair (formerly Director and Chief

Botanist, National Herbarium, New South

Wales), BR. N. Robertson (Director, Research

School of Biotogical Sciences, Australian Na-

31y

tional University), Lilian Fraser (formerly:

Chicf Biologist, Division of Science Services,

N.S.W, Department of Agriculture), Joyee

Vickery (formerly Scoior Botantsi, N.SW,

Department of Agriculture), N.C. W. Beadle

(formerly Professor of Botany, University of

New England), Gwenda Davis (formerly Asso-

claie Professor uf Botany, University of New

England), N, H. White (formerly Professor of

Plant Pathology, University of Sydney), and

Ilnva Brewer (née Pidgeon, School of Bio-

logical Scienzes, University of Sydney).

Osborn died after a short illness on 3 June

1973. He will be long remembered in Australia

Yor the mfluence he had on Botany im Adelaide

and Sydney, and particularly for his qualities

of leadership and inspiration of younger

people, He always had the huppy knack, even

m his later years, of being able to talk with

Students, lo be interested in what they were

doing, und to cutch their interest in his ex-

periences.

—R. N. Robertson and C. M- Eardley.

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