POST-EOCENE. HISTORY AND STRATIGRAPHY OF NORTHEASTERN

SOUTH AUSTRALIA

by H. Worsngk*

Summary

Woeener, H., (1974).—Post-Eocene Ilistory and Stratigraphy of (Northeasterq South

Australia. Trans, R. Soc. 8. Anst. 98(1), 1-12, 28 February, 1974.

The past-Eocene history of the central Great Artesicn Busin is characterised fy Jong

periods of aerial exposure interspersed with comparatively shorttived depositional events.

Products of deep chemical weathering on long exposed land-surfaces therefore palm ninjor

stratigraphic importance, equal to that of actually deposited rock-units.

To arrive at a meaningful and workable stratigraphy, a scheme is proposed which

combines conventional rock-units with morphologseal units of stratigraphic significances,

The sequence of events considered here commences with the CORDILLO SURFACE,

an aggradational plain which existed in the late Eocene ta early Oligocene. On this. plain

formed a “surface-quartzite*, the SILC REE OF THE CORDILLO SURFACE. The post-

Cordillo diastrophism deformed the Cordillo Surface and shaped broad fold structures, Im the

synclines of these structures the DOONBARA FORMATION, consisting mainly of tetruginous

sands and pisolites, formed. This formation is overlain conformably by the CADELGA

LIMESTONE, a chemical depesit of middle ta Inte Mioctene age.

Introduction

The depositional record of the ‘Vertiary

period in the central and western region of the

Great Artesian Basin comprises two compara-

tively thin sequences of fluviatile and lacustrine

sediments. The two depositional events were

separated by a period of exposure and non

deposition which was mitiated by widespread

epeirogenelic movements, These movements

not only formed the principal structural pat-

tern of broad aiticlines and syoclines 4s i]

exists today (Jack 1925, 1930; Wopfner 1960;

Wopfner & ‘Twidale 1967), but also strongly

influenced distribution and thickness of the

Tertiary deposits.

The first depositional event which com-:

menaced in the Paleocene und was terminated

ia the middle to late Eocene, comprises a

dominantly flrviatile and paludal sequence of

mualute sandstones with interbeds of line-

clustics and Tignites. This stratigraphic unit

which is now. termed EYRE FORMATION

(Wopfner, Callen & Harris 1974), was laid

down as an ulmost continuous sediment-

blinket, disconformably covering the under-

lving Cretaceous strata of the central. southem

and western Great Artesian Basin.

Sediments of the second depositional phase

Were first recoguised in the vicinity of Lake

Eyre and termed ETADUNNA FORMATION

by Stirton e¢ al. (1961). This formation con-

sists mainly of primary dolomites with inter-

beds of dotomitic shales and mudstones, Sub-

sequent results of drilling on Lake Eyre and

from Poonarunna No. 1, northeast of the

lake, has demonstrated an extensive distribu-

tion of this formation at shallow depth (Johns

& Ludbrook 1963; Wopfner & Twidale 1961).

Stirton et al. (1961) suggested an Oligocene

ze for the Etadunna Formation, but palyno-

logical data obtained recently by W, K. Harris

vf the Geological Survey of South Australia

from very similar dolomite sequences in the

Frome Embayment are indicative of a Miocene

age (Wopfner et al. 1974).

The distribution of the Etadunna Formation

ond iis equivalents is much less ubiquitous than

that of the Eyre Formatron, being restricted ta

the large downwarped areas of the Lake Eyre

region, the Strzelecki Desert and the Frome

Embayment.

The purpose of this present paper is ta dis-

cuss the events which followed the deposition

of the Eyre Formation in northeastern-most

* Geologisches Institut der Universitat Kéln, Z0lpicliersirasse 49, 5 Kaln, West Germany.

Formerly Geological Survey of South Australia.

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U. WOPFNER

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400 500 KILOMETRES

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iit

Fig, 1: Locality map showing major anticlinal structures in north-eastern South Australia.

South Australia. This region is characterised

by its large and often complex anticlinal struc-

tures and thus contrasts markedly with the

large, downwarped areas. This contrast is not

only evident in the different sedimentological

record but also in the development of altera-

tion products, resulling from chemical weather-

ing processes on long-cxposed land surfaces.

Such palaeosurfaces have therefore no less

stratigraphic importance than actually deposi-

ted sediments aid are treated here as morpho-

logical units of stratigcaphic significance.

Type localities and places and structures

mentioned in the text are indicated on Fig. 1.

Cordillo Surface

GENERAL DESCRIPTION

This new name is. introduced to identify that

land surface which existed in the early Tertiary

POST-EOCFNE HISTORY OF N.E. SOUTH AUSTRALTA 3

shortly before and after the termination of the

deposition of the Eyre Formution. This land-

surface developed over the whole central and

western region of the Cipeat Artesian Basin but

also extended westward well beyond the

basin margins (Wapfier 1967).

Termioation of the deposition of the Eyre

Formation, and consequently the development

af the Cordillo Surtace, was however not a

spomaneous event. Within the central Great

Artesiun Busin deposition ceased first in those

regions Where, due (vu epeiroyenetic instability,

jinticlinal structures began to farm. This struc-

tural growth which followed a pre-existing pat-

tern of fold structures already established in

the Permian (Woptner 1966; Martin 1967;

Kapel 173). is demonstraled by the overall

thinning and lensing out of the Eyre Pormna-

Hou aergss the crests of those aniielines

(Wopler ef wi 1974). This left some of the

unticlinal crests “hald-headed", exposing Win-

fon Fornmtion to the processes of weathering.

The rivers which were responsible for the

deposition of the Eyre Formation were thus

deviated into rhe svaclinal areas where sedi-

Invhlaviad contmued en vast Mood plains and

Mm iterititlent lakes and swamps. Depositional

regression g7adually reduced the area of this

carly Tertiary phase of sedimentation to such

wn exient that most of the region remnined as

astable and, fo all mtents and purposes, far

land-sorFace

Vhs stable surfiee of the late Rocene aud

carly Oligocene ms here ienmmed CORDILLO

SURFACE.

SUCKEL) ar the Cornito Sturpace

On the Nat and stable Cordilla Surfuce, lat-

eril rin off Was al a minimum, Coupled with

& high groundavater duble caused by the

depositioual regression, conditions existed

whieh led te deep chemical weathering and the

development of a leached soil-protile. Appar

ently within the B-horizon of this profile silien

hezan to accumulate in irrecular nodules which

then uselutinated into rod shaped aggeresates, 2

to 4 om thick and 15 to 30 cm long. As the

prolile matured. silica concentration imereased

lurther to form centripetally oriented colunrms

or polygonal prisms of a dense and brittle sil-

crete, The silerete. which may be up to 3 m

thick, grades downward into a zone af angular.

broken-up parent rock und this is underlain hy

leached and kaolinised. bur otherwise undis-

lured parent rock (Wopfner 1964: Wopfner &

Twidale 1967),

Tl is proposed that this Silerete be referred

tuas SILCRETE OF TILE CORDILLO SUR-

PACE.

The Silerete of the Cordillo Surface is com-

posed entirely of quartz, Whereby detrital

quartz grains and pebbles of the original rock

are still renunecd in their original shapes,

eneased in a microcrystalline quarte-nmatrix,

This contrasis with younger sileretes, like red

and white silic¢ified breveigs, silicified ¢arbon-

ales and opaline layers, in which tridimitic-

eristubaliue silica prodommates.

The Silerete of the Cordilla Surface is

ustilly best developed neue the erests and on

the flanks of the surface anticlines. Alone the

lower flanks of the wnticlines where the Eyre

Formation occurs in an all-tap position, sey-

eral layers of immature silerete niay be inter

ealated in the sediment-sequence, whereas a

mature sflerete usually caps the secuon. This

May indicate temporary “instability? of the

surluce when the formation of a silcrete-

profile was terminated hy the deposition ol

vew sediment on lop of ir.

Brom the limbs of the anticlines the silerele

commonly can he tpaced below the present

surface where its presence can cause great

difficultics during drilling operatens und is

therefore invariably vrevarded by the driller,

In the deeper synching! parts of te basin how-

ever, the silérete i$ oflen ubsent or its develop

ment is so rudimentary that it can he over-

looked very vasily.

ft would appear thetelore thal the fornmarian

of the silerete of the Cordillo Surface vom-

Menced in lhe crestal revion of the embryonic

amfeliaes whenve its development progressed

oulwards as lopeer areas heeame excluded

from sedimentation Thus the silerele way Just

but usually alsa least developed jn those areas

Where sedimentation persisted lonuest,

Tyre ARMA AND SroVioNw

The type area for the Cordillo Surface is the

Corlilio and Innamineka regsion where this

surface was first recognised, Por ohvicus

reasons ho type seclion can he estublished, but

Figs. 2 & 3 show typical expressions of this

surface,

The type section for the silerete of the

Cordillo Surface and the associated deep

weathering profile is Situated on the head-

waters of the central tributary of Jiblie Crock

where a compleie, monogenetic profile is

exposed on the cast face of a tall mesa, stand-

ing isolated in front of the Nappamilkiec esearp-

ment, Other sections more readily accessible

. WOPFNER

Fig. 2: Typical expression of silerete-capped Cordillo Surface on north limb of Innamincka Dome.

The silcrete capping forms the sharp edge at the top of the escarpment and is characterized by

an even, almost textureless pattern on aerial photographs. Scarp-foot erosion from the south

(left) has cut deeply into the northern limb of the dome, whereas a consequent drainage still

prevails on the north-dipping Cordillo Surface. View is to the WSW from a

South Australian-Queensland border.

exist in the vicinity of Needle Hill and on

Innamincka Dome (Fig. 2).

The name is derived from Cordillo Downs

station which occupies the northeast corner of

South Australia. Cordillo Downs homestead is

built on the south-dipping, silcrete-cove ed

Cordillo Surface.

DISTRIBUTION AND LATERAL DEVELOPMENTS

The Cordillo Surface can be recognised in

all structurally positive areas where it forms

the dip slopes of anticlinal structures (Figs. 2

& 3). It extends over the whole northeastern

corner of South Australia and the adjacent

structural uplands in southwestern Queensland

(Wopfner 1960). From the Cordillo anticlinal

complex it can be traced westward through

Sturt’s Stony Desert to the region of the Birds-

ville Track where the surface gains prominence

again in the Mt. Gason Dome.

It is also prominently developed on the

Innamincka Dome (Fig. 2) and on the Tick-

erna Structure.

point near the

{t cannot be traced with confidence beneath

Lake Eyre but equivalents of the Cordillo Sur-

face exist in the Oodnadatta and Dalhousie

region, where in parts it may be developed on

Lower Cretaceous strata. From here on west-

wards, the surface progressively —transsects

older rocks (Wopfner 1964), including Lower

Palaeozoic sediments and granites, exposed

along the margin of the Great Artesian Basin.

From these relationships it is apparent that

the Cordillo Surface and its equivalents may be

regarded as a depositional plain within the

area of the Great Artesian Basin, but as a

peneplain near the basin margin and beyond.

The geomorphic form of this surface indi-

cates that the system was exorheic, and open

to the sea in a southwesterly direction—a situ-

ation similar to that proposed for the drainage

pattern during the deposition of the Eyre

Formation (Wopfner et al. 1974). An exorheic

system may be indicated also by the fact that

remnants of silcreted surfaces can be traced

all the way to the shores of Spencers Gulf on

POST-EOCENE HISTORY OF N.E. SOUTH AUSTRALIA $

Fig. 3:

West limb of Haddon Syncline, showing marked east-dip of silcrete-covered Cordillo Sur-

face. Flat-lying Doonbara Formation (in background behind and to the left of tree) uncon-

formably laps onto the folded Cordillo Surface. Some columnar silcrete is exposed in right

foreground. The type section of the Doonbara Formation is about 1 km to the south of this

location,

Yorke Peninsula. The map of silcrete distribu-

tion produced by Stephens (1971) also sug-

gests an open system. However, it should be

noted that the age suggested by Stephens for

the silcrete formation is demonstrably too

young.

Mid-Tertiary (Post Cordillo) Diastrophism

Epeirogenetic movements which had made

their presence felt during the deposition of the

Eyre Formation became active again in the

middle of the Tertiary. The exact time of this

event cannot be ascertained as yet. The infor-

mation available at this stage indicates an

interval with a lower limit in the early Oligo-

cene and an upper limit in the early Miocene,

during which these movements could have

taken place.

The movements resulted in further folding

and warping in the deeper parts of the basin

and in normal faulting along the basin-margins.

The deforming forces acted in the same sense

as those which had been active during the

early Tertiary, thus reactivating structural

growth along pre-existing patterns. This led to

the development of large, commonly closed

anticlines with structural reliefs of 90 m to

200 m (Wopfner 1960),

Within the deeper parts of the basin, these

diastrophic forces appear to have acted rather

uniformly, resulting in slow but continuous

fold-movements. Along the basin margins

however, the same diastrophism was expressed

by a sequence of pulses which, depending on

the local stress-accumulation, occurred as

short-lived events in different parts of the

basin at different times. This is indicated by the

considerable variations in the maturity of those

sileretes of the Cordillo Surface which were

tilted or otherwise deformed by faulting along

the basin margin. Good examples may be

observed along the Mt. Harvey and Mt. Mar-

garet Faults south of Oodnadatta and the War-

ratta Fault southwest of Tibooburra. As such

strong deformation of these silcretes disrupted

the balanced morphological and groundwater

conditions required for the formation of these

silcretes, their stage of maturity also gives the

6 TL WOPENER

reluuve time of their deformation (Wopfner &

Twidale (967).

‘There can be litthe doubt, if any, that the

Cordillo Surface was actually deformed by

folding. tt can be shown in many places that

the planar contact between the late Cretaceous

Winton Formation and the early ‘Tertiary Eyre

Formation sirikes und dips i sympathy with

the Cordillo Surface, although the dip on the

latter may be one or two degrees less than that

observed at the base of the Tertiary, This indi-

cules quite clearly ihe common deformation

of both plones. Exeellent examples of this

were deseribed from the Innamineka Dome!,

the Hidudon Syneling aud the Morney Dome

(Wopfuer 1960), The Cordillo Surface was

also sed as the structural datum for the aerial

mapping of the central Great Artesian Basin

by the author and Dr. BR. 0, Brianschweiler

in 1957, Using the altimeter of the aircraft to

(measure the elevations of the folded Cordilfo

Surface, w structire-contour map was praduced

ol all the major surface sltuctures between the

Grey Range i western Queensland and the

Suppson Desert in South Australia (sce Sprigs

1958). Extensive acismiec and geolagical sur-

vevs carried out over Ihab area singe then have

proved! this iaph essentially vorrect, fhus con-

firming the basic morpho-stmitigraphie concept

outlined above,

Phe post-Cordillo diastrophisot cemplelely

reshpped the marpholagy of the central and

western Cifeat Artesiun Basin. ‘This changed

tuorpholowy, which ts andl the basis for the

Ustibuion of the mayor lanid-lorms of today,

also had @ promauneed effect on the drainage

and thereby on the sediment distribution. The

once vast and monotonous plains new heeame

sub-divided into distinctive morphological und

stroctural units Apirt from the various fold-

structures mentioned before, two lurge areas of

deposition commenced to take shape: one

formed in the region of Lake Eyre am! the

southern Simpson Desert, und a second one

developed in the area of Lake Blanche «and the

Strveleeki Desens The (wo negitive areas were

separited by a chain of antictines which

formed along the region now traversed by the

Hirdsyille Track. It would appeur cherefore,

that tus period of mid-Tertiary diastrophism

also farmed the mould out of which developed

jhe present endorheic drainage system of Lake

Eyre and Lake Fromme.

Doonbara Formation

GENERAL DESCRIPTION

As the unticlines rose above their suerournd-

ings. intial erosion gouged shallow, cunsequent

Urainuge systems into the flanks of the struc

tures. The eroded material wus deposited in

the neighbouring synelines, the sand-fraction

lose to its place of origin ani the finer grains

in the rhore distal segious. Reworked silercte

of the Cordillo Surface, ranging in purticle-

size trom course sund to cobbles, was fre

quently incorporated, purticidarly near the bise

of the sequence.

The formation of bread ind shallow drain-

age channels rather thin deep erosional incis-

ions Suggvests wat the area as a whole was tol

elevated much above base-level. The lowering

by erosion of the leadwater regions, coupled

with ihe gradual filling up of the depositional

areas, resulicd in a further and progressive

reduction of dynamic tntensily. Erosianal

vradients were thus reduced to such a degree,

that the landtorms heswne qudasestabilised,

This allowed for the cornmencement of ferral-

lisalion, a process which was particularly effec-

tive within the syoelinal regions, where high

groundwater levels were Tkely to have existed,

Ferralitisation, however should be envisaved as

a contionwos. almost syo-depesmanal event

Which acjustul lo new levels whenever new

crosunal detritus was mlded onfe an esting

surface

The result of this combination af deposition

und soil-precess led to the formation of ferris.

gingus ypisolites, pisolitie sandstimes and in

places to ferrngingus aolites. Tr is proposed

here ta term this. sequence the DOONBARA

FORMATION. The hase of the Doonhira

Formation is defined by its unconlormable of

disconformable contact with the silecete of the

Cordillo Surface of older rocks (Pig. 4),

whereas the top is placed below the first car-

bonate-hed of the overlying rockeurit,

Linio.osy

The Doonhirs Formation 1s subswintially a

brick-red, medium-grained, ferrginous sanil-

stone, large parts of which show pronounced

and well developed pisolitic texture. ‘The clas-

tic components consist almost entirely of

quarty grains which ore generally rounded to

subrounded gnd polished. Sorting is usually

good and il is suspected thitt a large proportion

| Worrnce, BH. (1958)—Vhe Geology of the Ionamincka Dome. Report for SANTOS Ltd a S. Aust.

Dept. Mines Fovel, 74. Unpublished,

POST-EQCENE

HISVORY OF N.E. SOUTH AUSTRALIA

Fig. 4: Typical flat cake of ferruginous pisolite of basal Doonbara Formation, resting on reworked

and fragmented silerete of Cordillo Surface. Silcrete-clasts are cemented with ferruginous

material derived from the Doonbara Formation.

km east of Cordillo homestead.

of the quartz grains have been derived by

reworking from the underlying Eyre Forma-

tion. In those parts of the section which have

not been affected by the formation of pisolites,

current bedding is often discernible. It is

usually a shallow trough-bedding with indivi-

dual sets averaging 15 to 25 cm thickness.

Near the base of the formation the grain size

increases to coarse sand. Granules and rounded

cobbles of silcrete are also common, An off-

white pebble conglomerate in coarse sand-

matrix may be present at the base of the

formation.

The pisolitic portions of the Doonbara

Formation occur either in thick, flaggy banks

or in the shape of round, flat cakes with dia-

meters ranging between 40 and 90 cm (Fig.

4), The usual colour is again brick-red,

although medium brown and dark yellow are

also common. Marked colour-differences are

often observed within the cake-shaped portions

of the formation, where the cake is often dark

red and the surrounding pisolitic material of a

much lighter, often bleached appearance.

Locality is at Nilpie Nilpie Creek. about 50

The individual pisoliths vary between 0,5

and 2 cm in diameter. They are generally mas-

sive, although concentric structures are present

in some areas. In cross-section the pisoliths

show a ferruginous, largely goethitic matrix,

enclosing fine to medium grained quartz. There

is normally very little clay within the pisoliths.

Frequently the inside colour of the pisoliths is

much darker than the surrounding “matrix”,

Cementation between the pisoliths is poor, giv-

ing the formation a very high porosity and

permeability.

The quartz-content of the sandy portions of

the Doonbara Formation is about 80 percent

but it may be less than 60 percent in the iron-

rich pisolitic portions. The average contents of

iron and alumina also yary over a wide range,

A number of analyses of pisolites from the

Doonbara Formation (then referred to as “fer-

ruginous pisolite’), were presented by Wopf-

ner & Twidale (1967). These analyses show

that despite the wide range of the individual

values, the ratio between Fe.O. and Al,O,,

remains fairly constant at about 0,3.

# H, WOPFNER

Immediately beneath the base of the Doeon-

bara Formation ong observes 4 kind of rezo-

lith, where the underlying, older rocks have

been broken up and disintegrated info angular

lrayments. The interstices between the rock

fragments are cemented with red, ferruginaus

material derived from the overlying Doonbara

Pormation, Still further below the contact, a

pronounced red and white mottling in the pre-

Doonbara material is developed, In many

instances the hase of the Doonbara Formation

cun be seein (rans-secting from silerete onto

sediments of (the Eyre Formation or even

older rocks, clearly demonstrating the erosional

and disconformuble relationship between the

Doonbura Formation and the underlying

stratigraphic urls,

Tyr AREA AND Seciion

The type area for the Doonbiura Formauon

is the northeastern-miost portion of South Aus-

iralla, in particular the immediate surroundings

of the Cordillo Structures, the Tonantingka

Dome and their extensions into Queensland.

The type section is situated on the COR

PIT) 12250000 nrap-wrea. about 70 ki

north of Cordilla Downs homestead. where

about 8 moot dark red sandstane and pisotite

are exposed on the western limb of (he Haddon

Syneline (Fis. 9). The locality is almost he

west of Narrartell(i waterhole. Additiomul tofor-

mation on the sequence was obtitned from seis-

mye shop hotes. dled aeross the Haddon

Svneline (Wopfner 1960)-

Avy excellent seclan also existy at Candra-

decku walerhole on the northwest limh of the

Invamninteka Dome (IS NAMINCKA 12250 000

mapedredy, Phos section whieh was described

in some defail recently 16 selected ay a reference

section®

Vhe name of the formation derives from

Doonbary Well, situated ou the west linth of

Ihe Nuppaniikie Antiing (Wepfoer 1960).

and some 60 km north of Cordilla Downs

homestead. The well ohigins its water from. the

Doonbary Formation (Wopfaer 1961).

Dist Rib iow AND AGE

The Doonhara Formation is ubiquitous

along the Munks of all the major surface anti-

clines, Whence it extends inte the subsurface

(Wopfner 1960, 1961). It is generally present

within the synelinal structures where it is

usually covered by younger deposits. The

average thickness observed in outerop is about

7 to 15S m, but i some areas it may be con-

siderably thicker. The maximum thickness

revorded sa fur is 40 m iw the core of the

Haddon Syacline (Wopfner 1960).

Locally the Doonbara Formation provides

the reservoir for the run-off from: occasional

precipitation and forms an aquifer on the

slopes and peripheries. af the anticlinal struc:

tures. In proximity to local (take areas the

water is of excellent qualily (Woptner 1961)

From the surluce structures ih oortheastern-

most South Austtalia and western Queensland,

the Deonbura Formation can be traced west-

ward under Sturts Stony Desert Occasionally

the formation is exposed ow the surface us for

instance north of Beckwith Swamp and on the

castern slopes ol the Mt, Guson Uplift. Ferru-

winous pisolites und ovlites at the base of Lhe

Btadunta Formation in the Lake Fyre bores

(Johns & Tantbrook 1963) are regarded hy

the present author as equivalents of the Doon

hata Pormation (see Wopfner & Twidale

1967),

The value of alumimous hlerites: as strau-

gtuphic marker horizons was ported oul most

recently hy Valeton (1972). Sinee terratilisa-

lion also frequives rather specialised climatic

and morphological condhons. i would appear

reusonuble ta use this criterion as @ basis lor

correlation

To the northwest of Lake Evre, litholagieally

identicul sequences are aeain exposed alone

synelinul areas between Qodhadatla and. the

Norther Territory border. Extensive renmants

also occur onthe Lleatanna platedu COODNA-

DATTA 1:250 000 map-areny und on the

Emmery Kinge (DALHOUSIP 1:250 000)

map-rren)

No fossils have been found Wt the Dounhara

Formation so far and iis uge 1s nol kiown

With certainty. However. if the correlation

with the ferruginous. oolites ait the base of the

Etaduona Formation is correct, an approsi-

mute age Gain he deduced. Recent palynological

work by Horris (see Woptner er al, 1974)

indiciwtes uo Miocene agé for the Eraduona

Formation, From this a late Oligowene or carly

Miouene ape seems to he most likely for the

Doonhara Formation.

Cadel Limestone

GeNeRAL Deserir fon

A thin sequence of carbonates overlies the

Doonbura Formation in many places. The

*THors ran, BR. C.,

Aust, Kepl. 73/26,

(1974).

Unpublished

Mousured Seetions from the Innamineka 1:250 000 area, Ceol, Surv. 5.

POST-EOCENE

lypical ltholoyy of this ecarbouate sequence,

comprisiny pale coloured, cherty limestones

anu dolomitic limestones, remains remalkably

Uniform over large areas of the central and

Weslern Great Arivsuin Basin. It is proposed

here to uune Min curhomite sequence the

CADELGA LIMESTONE, The lower boun-

dury of this unit as delined by is contact with

the underlying Doonbara Formation whereas

the upper limit ts usually formed by an ero-

sonal surhice

The contict between the Doonbara Forma-

ton and the Cadelew Limestone generally

uppears to he conformable. although toa wun,

her of exposures a disconformable relationship

is Suuvested by marked crosiaiial features al

the base of te carbonate cleposits, Erosion

must be expeeted at this bauudary which marks

the chinge from the subseren! deposition and

ferratitisation under which the Doonbara Vor-

tation Was formed ane the subaqaeous envir-

onment in which the Cadelyu Limestone was.

hud down,

Where the water came trom which provided

the medium for the deposition of the Cadelya

Limestone is Sui highly speculative. From the

Widespread distribution of this limestone und

is cquivadents, esiending from western Queens -

land to Westeru Austhivia. ane would be justis

fied in accepting ether permanent or tidal

Mundation by sea-water a4 suggested by Toye

(1968), provided a satisfactory explanation

can be found for the almost complete absence

of maring fossils (see below), It was mentioned

carlier that the landscape which existed at the

time of deposition of the Doonbara Forniation

Was not much elevated ahove base level, If

this base level was sea level, even u small flue

tuation of the Jatter would have inundated

large areas, in particular the synchitral regions,

to Lorn chains of shallow pans and lagoons.

The paucity of clastic ovatenal together with

Ihe abundance of dolomite, chert and algal

structures is indicative of a mildly evaporitic

environment, and hypersalinity would thus

account for the near absence of marine fossils,

Allernalively, only slight variations would he

required to udjust the above model to an

endorheie system of similar or identical morph

ology which Was never or only rarely con-

necled with the sea, [In this case the occasional

foraminifera could have heen brought in by

hirds, whereas larger animals could have

enited ecess via lemporary interconnecting

channels

HIShORY OF NE.

SOUTIT AUSTRALIS ”

Liriacocy

It is Vory difficut to find a surface exposure

ot the Cadeloa Limestoue which m nor reduced

by erasiou. However, the dominant litholowies

constituting this stratigraphic unit are so vhur

acteristic that they ean be recognised and

readily icentitied i widely separated localitivs.

Jn the type seetion about 4 om of Cudelya

Limestone q'e exposed, The lower pure of the

section consists of fawn lo pink. ehulky lime-

stone, containing a great abundance of

reworked tragments of the underlying Doon-

bara Formation. This reworked material nuiges

in size [rom individual, goethite-coared quarte-

erains to fragments und aggrevates. of pisohites

ubout 2 10 3 em in-diameter. These limestones

are interbedded with olive green. silty shale,

calcareous shale and thin carbonate-bands,

Lenses of red, sandy limestone are also present

Outside the type section one observes at thes

level also banded limestones, consisting of

alternating crewnr and maroon or purple bands.

several centimetres thick. ‘This rock-type was

also reworked itd is then found, forming

aagulor fragments up ta 2 em thick and 5 om

Jong, am slightly tizher portions of the

sequence. Vugey limestones are also common

in thiv lower purt of the succession. On the

southern flank af the Cordillo Dome, in the

lower reaches of Nilpie Nilpie Creek, some

round and fibrous structures, about | to 2

em in diameter, up to 25 cm long and irceger

lacly curved, are observed om the bedding

planes. ‘These strictures are thought to be

culctfied algal colonies.

The middle and upper parts of the sequence

consist of thickly-bedded to flazgy limestones.

usititly of fight grey to beiwe colour. ‘These

are hard, brittle and dense carbonutes, rang-

ng In composition from slightly dolomite

limestones to dolomites. All ot these eomain

Jenses, wisps amd irregularly shaped bodtes of

whit grey and black chert. Some of the

cherts are banded and show depositional fea:

(wes Indicative of primary cheris whilst ethers

wppear lo have replaced the original carbonate

during disgenenis. This latter ovcurrence may

hest be expliined as a nucleation effet

Usually the ¢herts are amorphous, consisting

of tridimitic and cristobalitic silica. but reerys-

lallisution is reasomibly common an same parts

When exposed to weathering the carbonate

dissolves, leaving Ihe cherts to form rent and

Tugged remnants on the surface of the rock

(Fig 5). In some instances where the carbon-

ate has been renioved cornpletely, the eroured

10 H. WOPFNER

Fig. S:

Exposure of Cadelga Limestone at the type section, about 7 km northeast of Cadelga water-

hole and just south of the border fence between South Australia and Queensland. The dark

portions on the otherwise light coloured rock in the left and central foreground are stringers

and irregular patches of chert. Hammer handie measures about 25 cm,

surface is covered with residual chert frag-

ments as the sole indication of the once present

Cadelga Limestone.

The carbonates are generally micritic, but

dolo-siltites and calcarenites are also observed,

Dark grey to almost black, bituminous lime-

stone occurs near Horseshoe Well. on the

southern limb of the Cordillo Dome. Apart

from the possible algal structures mentioned

above. some gastropods and (?)diatoms were

observed in thin sections, made from material

from the CORDILLO 1:250 000 map-area.

Based on the lithological and textural char-

acteristics outlined above, it is suggested that

the Cadelga Limestone is largely a chemical

deposit which was laid down in large, shallow

pans. The dolomitic nature and the abundance

of chert indicate a mildly evaporitic deposi-

tional environment.

lyepk AREA AND SECTION

Phe type area for the Cadelga Limestone is

the region around the Cordillo and Innamincka

structures and Sturt’s Stony Desert. The type

section is situated on the area of the COR-

DILLO 1:250000 map-sheet, about 13 km

north of Doonbara Well and on the western

limb of the Nappamilkie Structure (Fig. 5).

The name of the formation is derived from

Cadelga waterhole, situated approximately 7

km southwest of the type section. Cadelga

Limestone occurs in the immediate vicinity of

the waterhole and grey and white cobbles and

pebbles of chert with a typical smooth, lustrous

(“greasy”) surface appearance were concentra-

ted by selective erosion along the northern

bank of the waterhole. According to aboriginal

legend, these chert-pebbles are the fat which

was splattered by the ancestral goanna when

he went hurriedly underground to escape the

chase by the kangaroo man. The hole which

formed where he went down is now Cadelga

waterhole. The cherts associated with the

Cadelga Limestone were of considerable im.

portance to the aboriginal inhabitants of that

region, Who valued them as an excellent raw

material for the manufacture of stone imple

ments.

MOST-EOCENE HISHORY OF NE. SOUTIT AUSTRALIA iI

DisiRmuTION AND AGE

Cadelga Limestone ts exposed intermittently

wlong the westeris and southern limbs of the

Cordillo structure, in the Haddon Syneline and

the northern part of Sturt’s Stony Desert. Ir

occurs also on the north limb of the Inna-

mincka Dome and in the Patchawarra Trough,

where it is covered by younger sediments,

From here jt may extend below the surface

into the area of the Gidgealpa and Moomba

gas fields, where chalky limestones and cherty

dolomites are folind above the clastic sequence

of the Fyre Fornration. These carbonates are

thought to be. at feast in parts, equivalents of

the Cadelga Limestone. From there to the

south-west, the same carbonates. are then cor-

related with the Ftadunna Formation of Stic-

ton vt al. (1961) and with Miocene carbon-

‘tes in the Frame Embayment (Wopfner et al,

1974).

Chalcedonic limestones of identical lithology

ry the Cadelga Limestone are exposed on the

West shore of Lake Eyre, near the mouth cf

the Neales River, an occurrence which,

jhrough its proximity to the Etadunna Forma-

tion beneath Lake Evre (Johns & Ludbrook

|963}, strengthens 4 lithological correlation

between Lhe Cadelyo Limestone and the Eta-

duntu Fermation.

Lithe-cquivalents of the Cadelea Limestone

are widespread alsa belween the Simpson Des-

ert and the western margin of jhe Great Artes-

inn Basin, In the Oodnadatta region they are

referred to as Alberga Limestone (Freytag e:

vi. 1967), Undquestionable fests of foramini-

fera were Found by the present author tn thin

sections of Ajberea Limestone From a locality

neat MA Alice.

As tuentioned above, the only fossils

tecurded [ram the Cadelga Limestone so far

ure some yastropods, (?)diatoms and algal

sttuclures, None of these are sufficiently diag-

mastic to establish the aga of the sediment,

Based on the correlatron with the Etadunna

Formation, 4 middle to late Miocene age is

suygested tor the Cadelga Limestone,

Conclusions

Recognition and definition of post-Eocene

sedimentiry and morphological units allows

the reconstruction of the geological history af

the northeastern portion of South Australia

and adjoining parts in Queensland. This his-

tory is characterised hy a topography of low

amplitudes, thin sedimentary sequences and a

plonolinced presence mf alteration products.

Throughout the period under consideration, the

region €Xperienced fettenic stability, except

for the period of epeirogenetic movements

{post Cordillo diastrophism) ty (?)late Oligo-

vene tw early Miocene time.

The depositional periods described here fol-

lowed the diastrophic movements and major

depositional areas were established in the syn

clinal and synectiform depressions formed by

these movements. Such dependence of sedi-

mentation on structural events as indicated hy

the reciprocal thicknesses of the carbonates

(Cadelya Limestone, Etadunna Formation and.

equivalents) and the Doonbura Formution can

be interpreted as due to longer exposure to

aerial conditions, and thereby later inundation

of the vegions proximal to structurally positive

areas

If the total Tertiary sequence, jaclusive of

the Eyre Formation is considered, one notices

# remarkable similarity with other Tertiary

successions in South Australia, When coim-

piring the much more complete and largely

Marine sections of the coustal basins with those

sketchy sections from the very margin of

deposition, one must not overlook the fact

that only basic trends will remain to be com-

pared, and that long periods of time may he

represented by only a few metres af sedijnent

or just a palaeosol.

Of interest is the climatic history of the

region as indicated by the sequence of sedli-

ments and palacosols described m this paper.

A moist to seasonally wet and warm-temper-

ale climate 19 indicated in the early Tertiary

during the dvpasiliow of the Eyre Formation

(Wopiner et af. 1974), and very much the

same climate, perhaps with more pronounced

seqsonal aridity, can be precheted for the

silerete formation. The ferralitisation during

the period in which the Doonbara For-

mation was formed is indicative of a warmer,

probably hot climate with high rainfall, where

as increased artdity and warm to hot condi-

tions prevailed during the deposition of the

Cadelen Limestone:

Thus a temperature maximum is indicared

in the Miocene, with lower preceding lemperi-

tures jn the early Tertiury and a gradual de-

cling in the post-Miocene. This mid-Tertiary

temperature peak observed in Australia con-

trasis with the palaeo-climatic curves for the

Tertiary of Europe and North America, There

the temperature decreased steadily from ithe

Eorene onwards. until the minimum of the

Pleistocene glacial periods was reached. This

wus pointed out by Schwarzbach (1966), who

[2 ii. WOPFNER

suggested drifting of the Australian continent

to account for this discrepancy in the palaeo-

glimatic history of the Australian Tertiary.

Such u hypothesis, invoking a north drift of

the Austrulian continental mass in the carly to

mid-Tertiary is also in close agreement with

latest geological data obtained from Creta-

ceous-Vertiary basins along the southern cust

of Australia, and with palaeomagnetic results

trom Australian Tertiary volcanics and the

floor of the Soulhern Ocean.

At the beginning of the Tertiary the distribu-

tion of land-forms ia northeastern South Aus-

tralia was considerably different lo thiat

observed today. The basic distribution of

morphological units as it exists al present was

introduced by the post-Cordillo. diastrophism

ivy the early mid-Tertiary. Since the deposition

of the Cadelga Limestone, modifications.

occurred only by degree and the changes so

apparent in the late Cainozoic history of the

region can be ascribed exclusively to varia-

lions of the climute coupled with some minor

opeitogehetic re-adjustments,

References

Peevrac. 1. #, Urari, G. R, & Worrnor, H,

(1967), DODNADATTA map sheet, Geo-

logical Atlas of South Australia, 1:250 000

eerie, Sheet SGS53-15 zone 5. (Geol, Sury.

§. Aust: Adelaide).

lack. R, T.. (1925),—Some developments in shal-

Jow warer arcas im the northeast of South

Australia. Bull, geal Surv. §. Aust. V1.

Jack, RK, lL. €1990).— Geological stricture and

oiher Faclors in relation to underground water

supply in portions of South Australia. Bull.

geal Surv. §. Aust, 14,

Jouns, RK. & Tiinanoox, N. A. (19639) —tTavesti-

ayiion of Luke Kyre, Rept, Invest. geol. Surv.

a. Austr. 24,

Karec, A, J. (1972).—The geology of the Patch-

wwuten area, Cooper Basin J. aust, Perrel.

Explor, Ass. P20), 53-57, .

Lroyp. A, R, (1968).—Possible Miucene marine

transeression in northern Australia. In

Pulacontological papers, 1965. Bull. Bur, Min,

Res. 80, 85-102. "4

Martin, C, A, (1967) —A deseriptive summary

of Moomba. gastield. Australas. Oil Gas, J.

13( 12), 23-26,

Seuwanesacnh, M, (1966).—Das Klima des rhein-

ischen ‘Tertiivs, 24. deutsch. avol. Gey JLB,

43-68,

Sertcs, R, GC, ((958).—Pelroleum prospects of

western parts of Great Australian Artesian

Basin, Bull. stm, Ass, Petrol, Geol, 42, 2465-

2491.

Srepursxs, C. G. (1971).—Laterite and silerete in

Ausindia; A study of the genetic relution-

ships of laterile and silerete and their com-

pinion materials, and their collective -signifi-

eanee in the farmution of the weathered

mantle, soils, telief ond drainage of’ the Aus-

tralian continent. Geoderma 5, 5-52,

Stiaton, R., Teprouo, R. 1. & Mincer. A. A.

(1961).—Cenozmie stratigraphy and verte-

brate palaeontology of the “Tirart Desert,

South Australia. Ree, 8, ust, Mas. 14, 19-

OT,

VALETON, I. (1973)—Taterite als Leithorizonte

zur Rekonstruction tektonischer Vorgiinge

auf den Festhindern, Geol. Rdsch. 6241),

153-161.

Worrner, Ho (1960).—On some structural devel-

opment in the central part of the Great Ans-

tralian Artesian Basin, Trans. R. Soe. S.

Anst. 83, 179-193.

Worrner, H. (1961),—The occurrence of a shal-

low vroundwater horizon and its natural oui-

fots in northeastern-most South Australia.

Trans, R, Soc, S. Aust. 85, 13-18.

Worerser, H, (1964).—Tertiary duricrust-profile

on Upper Proterozoic sediments, Granite

Downs area. Quart, geol. Notes, geal. Surv-

S. Aust. 12, 1-3,

Worencr. IT, (1966).—A case history of the

Gidvealpa gasfield. South Australia, Afotra-

las. Oil Gas J. 12011), 29-53,

Worrner, 1. (1967)—Some observations on

Cainozoie fand-sarfaces in the Officer Basin.

Onart. geal. Notes, weal, Surv, §. Aust. 23,

3-8,

Woarrner. H. & Twiparn, GC. R. (1967).—Geo-

morphological history of the Eake lyre

Basin, Jn 4. N. Jennings & J. A. Mabbult,

Eds... “Landform studies from Australia and

New Guinewx”. pp. 118-143. (A.N.U. Press:

Canberra.)

Worrner, H., CALLEN, R. & Harris, W. K.

(1974),—The Lower Tertiary Fyre Forma-

tion of the south-western Great Artesian

Basin. J. geol, Soc. Aust. 21(1).

THE ORIGIN OF COTTONS BRECCIA, KING ISLAND, TASMANIA

BY J. B. JAGO

Summary

JAGO, J. B. (1974).-The Origin of Cottons Breccia, King Island, Tasmania. Trans. R. Soc. S. Aust.

98(1), 13-28, 28 February, 1974.

Cottons Breccia is the southernmost and most isolated of the proven and possible Late Precambrian

glaciogenic sediments of Australia. It outcrops over a distance of 8 km along the southeast coast of

King Island; it varies in thickness from 40 to 100 m. The lithology varies considerably,

both laterally and vertically over quite short distances. Cottons Breccia is a very poorly sorted,

crudely stratified rock with angular clasts set in a carbonate or limonite cement. Thin siltstone and

sandstone lenses are reasonably common. The great majority of clasts show some rounding

although some clasts show no sign of rounding. The largest clasts in any particular horizon are

generally 30-50 cm or less across. However, at one locality there is a 15 m interval of very large

carbonate clasts with the largest one being over 3.3 m long. The larger clasts tend to be quartzite

and the smallest clasts a variety of metasiltstones. However, on the whole, various types of

carbonates dominate the clast assemblage. Very rare basic lava clasts are known; no acid igneous or

high grade metamorphic rock clasts have been found.

THE ORIGIN OF COTTONS BRECCIA, KING ISLAND, TASMANIA

by J. B. Jaco

Summary

Jace, J, B. (1974),—The Origin of Cottons Breccia, King Island. Tasmania. Traas. 2, Sav,

A. Aust, 98(1), 13-28. 28 February, 1974,

Cottons Breccia is the southerumosl and most. isolated of the proven and possible Late

Precambrian glaciogenic sediments of Australia, It outcrops over a distance of 8 km alom

the southeast coast of King Island; it varies in thickness from 40 to 100m. The lithology varies

considerably, both laterally and vertically over quite short distances, Cottons Breccia is a Very

noorly sorted, crudely stratified rock with angular clasts set in a carbonate or Hmonite cement.

Thin siltstone and sandstone lenses are reasonably common. The great majority of clasts show

some rounding although some clasts show ny sign of rounding. ‘I'he largest clasts in any pat-

ticular horizon are generally 30-50 om or less across. However, at one locality there is a 15 m

interval of very large carbonate clasts with the largest one being over 3.3 m long, The

Jucger clasty tend to be quartzite aml the smallest clasts a variety of metasilistones. However,

an the whole, various lypes of carbonates dominate the clast assemblage, Very rure busic

luva clasts are known} no acid igneous or bigh grade metamorphic rock clasts have been Found,

Features such as drop-stones, thin sandstone lenses within the breccia, and the possibility

of varved sediments, suggest a glaciogenic origin for Cotions Breccia. The presence of graded

bedding, the crudely stratified nature of the breccia and the fuct that almost all the clasts vre

sedimentary suggest a densily flow origin. It is possible that Cottons Breccia originated in a

fectonically active area by a combination of glacial action and submarine masy transport,

Introduction

Dunn ef al. (1971) have proposed to use

the Late Precambrian glaciation of Australia

ag the basis of a contintent-wide chronostratt-

graphic unit, The southernmost and mest wo-

lated of the glaciogenic sediments noted by

Dunn e¢ al. (1971) is a tillite-like rock from

King Island (Fig. 1). ‘The regional geology of

King Island is shown in Fig. 2,

This reck, defined below as Cottons Breccia,

was first noted from City of Melbourne Bay

by Warethouse (1916) who cansidered it to

be a Permo-Carboniferous glacial till, Carey

(1947), while supporting a glacial origin for

Une cock, suggested a Cambnan age and corre-

lation “with the Adelaide series glacial horizon,

and iso with the Daspoort and Griquatown

tillites of South Africa’, Carey also suggested

that the overlying laminated dolomite may be

a varved sediment. Hills & Carey (1949, p.

23) included the King Island rocks within the

“Zechan Glacials” then considered to be of

Cambrian age but now known to he Permian

(Spry 1958; Blissett 1962). Hills & Carey

{1949) stated: “this formation includes o true

illite rich in striated pebbles associated with

varved shales”. However, it was not specifically

Stated that striated pebbles cume from King

Tsland although Hilly & Carcy noled striated

pebbles trom the Zechan-Dundas. area.

David & Browte (1950, p. 77) called the

tocks under discussion the King Island Beds

and assigned them to the Late Precambrian.

Banks (1956, 1962) and Spry (1962) agreed

with Carey (1947) and considered the King

Tsland rocks to be a tillite; Spry (1962) sug-

gested correlation with the Sturt TVillite of

South Australia.

Edwards ef al, (1956, p, 75) noted the

presence of irregular ovoid patches or “pods”

in the hanging wail of what they termed the

Top Orebody Bed of the King Island Scheelite

Open Cut. They further suggested (p. 77) that

these pod-bearing beds are the metamorphosed

equivalent of Cottons Breccia.

Bartlett (1962) called the rock a con

alomerate Without reference to its origin, A

map by Bartlett {p. 8 in Smith & Williams

1963) of the southeast coast of King Island

notes the presence ef tillite and dolomite

* Department of Applied Geology South Australian Institule of Technology, Adelaide. S.A, 5000,

I4 J. B. JAGO

4 Claciogenic sédiments

as Possible glaciogenic sediments

1000km

Fig, |. Distribution of proven and possible glaciogenic sediments in Australia (modified after Dunn ef

al. 1971).

breccia. Schwarzbach (1965) noted the uncer-

tain stratigraphic position of Cottons Breccia

which he regarded as being of possible Late

Precambrian age. In reviewing the possibility

of a world-wide Late Precambrian glaciation,

Harland (1964, 1965) included Cottons

Breccin. in the Late Precambrian tillites.

Solomon & Bartlett (in Solomon 1969) pro-

duced a generalized stratigraphic succession of

the southeast coast of King Island, They noted

the presence of striated pebbles and mapped

the unit concerned as a Lower Cambrian or

Upper Proterozoic tillite. Large (1971) used

the term tilloid to describe the rocks under

discussion which he included in the Grassy

Group. However, the Grassy Group was

named by Knight & Nye (1953, p. 1,222) as

“the contact metamorphosed sediments of the

mine and environs”, One of the problems of

the geolagy of the south-east of King Island

has been the difficulty in trying to correlate

from the City of Melbourne Bay arca to the

mine area, Wo satisfactory correlation is

available, and hence the term “Grassy Group”

should not be used for rocks outside the mine

area,

The terminology of sediments of possible

glacial origin has been discussed by various

workers (Schermerhorn & Stanton [9463.

Schwarzbach 1965, Schermerhorn 1966, Har-

tand et al. 1966, Cooper 1971, Kroner & Ran-

kama 1972. Rankama 1973). The terms till

and tillite have been used for « considerable

time for unlithified and lithificd glacial sedi-

ments respectively (Harland e¢ al. 1966),

Numerous workers (e.g, Schermerhorn &

THE ORIGIN OF COTTONS BRECCIA, KING ISLAND. TASMANIA 15

@Naracoopa

REFERENCE

QUATERNARY and TERTIARY

fs] aeouanire and LIMESTONE

CARBONIFEROUS

f+] GRANITIC ROCKS

() CAMBRIAN

SEDIMENTS and VOLCANICS

PRECAMBRIAN

GRANITIC: ROCKS

_-7See Fig:3

SEDIMENTS and LOW-GRADE

METAMORPHICS

City of Melbourne Bay

Fig. 2.. Geology of King Island (modified after Tasmanian Department of Mines map, 1961 edition).

Stanton 1963, Kréner & Rankama 1972) supg-

gest that the term tillite should be applied only

to rocks of undoubted glacial origin. Such

terms as tilloid, pseudotillite, diamictite and

maixtite have been used to describe tillite-like

sediments of doubtful or non-glacial origin.

There is no general agreement as to which

term, if any, should be used. In the following

definition and discussion the term breccia is

used because (a) it does not prejudge the

origin of the rocks of southeast King Island

and (by) it is a suitable descriptive term for

these sediments.

Definition

Cottons Breccia is herein defined as that

poorly sorted, crudely stratified rock, with

imgular clasts set in a carbonate or hematite

cement, which outcrops over a distance of

about 8 km along and near the southeast coast

of King Island between Lancaster Creek (lat,

39°57.2'S; long, 144°08.2'K) and Cottons

Mlat (lat, 40°01.5’S; long. 144°06.9’E). The

most common clasts are various carbonates,

yuartzite and metasil{stones. They range up to

3,3 m across. Cottons Breccia is overlain cither

conformably by a. siltstone or disconformably

by a dolomite or dolomitic siltstone. It overlies

a metasiltstone with apparent conformity. The

formation yaries in thickness from about 40 m

in the Robbins Creek/Cumberland Creek area

to about 100 m in the City of Melbourne Bay

area. The lithology varies considerably, both

laterally and vertically, over quite short dis-

lances. Hence, no type section is designated.

The unit is unknown away from {he southeast

coast of King Island. The age of the formation

is either Late Precambrian or Cambrian, Cot-

16 J. B. JAGO

REFERENCE

?LATE PRECAMBRIAN —?CAMBRIAN

c volcan

v_v_} Basic volcanics

Dolomite, dolomitic siltstone,

siltstone and shale

o © | Cottons Breccia j

Ne t Lancs

Dolerite SSter Cree

[| Sandstone and siltstone

—— Fault

he Gut

Creek

Cottons /o 2hag

Flat o//

Fig, 3. Geology of part of south-east coast of King Island.

THE ORIGIN OF COTTONS BRECCIA, KING ISLAND, ‘IASMANIA 7

fons Breccia tf oamed after Cottons Creek

which enters the “ew at lat 40°01.4'S; long,

144°07.1' ER.

Age at Rocks

By comparison with similar yoleanics from

western and northwestern Tasmania, the vol

Cunics assocmied with the breccia suggest a

Cambrian age (Carey 3847, Scott 1951, Solo-

mon 1969}. Mowever, the age of the base of

the essentially Cambrian volcanics in Tas-

mania is unknown; it could be asx old a® the

Late Precambrian,

There is ulso the reverse argument, ic, if

the breeela is indeed one of the Late Precam-

brian tllites and that these fillites represent 4

chronostraugraphre unit as suggested by Dunn

et al. (1971), then the essentially Cambrian

volcanism of Tasmania would have started in

the Late Precambrian. The volcanics from

King Island have not been dated radio

metrically, 1 conducted an unsuccessful search

for fossils m the sediments overlying dhe

breccia,

The only tocks dated radiometrically on

King Island are those reporied by McDougall

& Legeo (1965), These workers concluded

that the granitic racks of the west coast of

King Island were most probably emplaced

about 750 ma. If (he sedimentary rocks in-

truded by granite on the west coast are con-

formably overlain by the sequence centainiog

the breccia on the east coast, then this would

suggest a Precambrian age for the breccia. An

alternative explanation is thai ihere is an un-

conformity betwcen the sequences exposed on

the west anc cast coasts of the island (Gres-

ham 1972; Geopekn Ltd., unpublished report)-

However, over most of King Island away from

the coasts, a thin veneer of Quatemary sedi-

ments obscures the underlying rocks,

Thus, at present there is no direct evidence

for the age of the breceia.

Present Investigation

In order to attempt to determine the origin

of Cottons Brecetu, 9 days were spent on King

Island between December 28, 1972, and

January 5, 1973, The geology of the area

undec discussion is shown in Fig. 3. The

breceia is exposed along the south-east coast-

line between Cottons Flat and Lancaster

Crock over a distance of abnut. 8 km The re-

lationship between the geology of the area

shown ls Fiz, 3 and that of the mine area

(immediately south of Fig, 3) & unknown

The breccia appears to be cot off at both the

Worth aid south by faults.

Simligraphic sections were measured across

the breeeta ar various points (Fig. 4). Where

possible the sections Were ammeasured from the

base of the overlying massive voleanics, down

through the siltstones and breccia to the wnder-

lying dolerite intrusion or sedimentary rock,

However, at many localities even the top of the

breecia was maccessible due to the sea. Once

away from the shore platform, outcrop is very

poor except in the gorges of Cuntberland and

Robbins Creeks. In the southernmost outezops

in the Cottons Flat avea, neither the lop mor

the bottom of the breccia could be Jovated.

although general stratigraphic considerations

suggested that the base of the outcrops in this

atea Were close ta che base of the. breccia, In

most sections the breccia appears to conform-

ably overlie u fine quartzite or metuasiltstone.

However, in Robbins Creck it directly overties

dolerite, In most sections a dolerite mtrusion is

found only a Jittle way below the base of the

breccia.

In some localities (e.g The Gut) the

breccia 1s overlain with appansnt conformity

by a fine red hematitic sandstone (Figs. 6 &

7), a Jamifated red sillone or a fine preen

siltstone, However, at one locality abawt 100m

south of Shower Droplet Rock the laminated

dolomite directly overlies the breccia with

clear evidence of disconformity between the

breccia and the dolomite (Figs. 8 & 9), In

hoth Figs. 8 and 9 the busal part of the dolo-

mite is clearly conglomeratic (particularly Fig.

9}.

In the two northern sections (Cumberland

Creek, Robbins Creek} the situation is dif-

ferent. In both sections the main body of

breccia is overlain by about 3.5 m of a hard,

green Ivminuied dolomitic siltstone which In

Robbins Creek contains a few pebbles } in 2

em across, This siltstohe is in tur overlain

by about 1.5 m of fine breccia. In Cumberland

Creek this “upper” breccia is overlain by about

3 m of pebbly sandstone before passing up

into ar least 8 m of well-bedded, purplish silt-

stone and dolomite, Jn Cumbertand Creek

there tf no more than 43 m of section between

the top of the breccia and the base of the

avetlying massive volcanics.

In the other sections whore the sediments

above the breccia and averlying thin siltstone

are exposed, there are between 3 and 12 m of

laminated dolomite Which in places is pyritic.

This is followed by between 20 and 35 m of

Ls 1 & JAGO

lominared grey, green, and black siltstones ant

shales, some of which are dolumitic or pyritic.

At some localiti¢s there are volcanic horizons

(tufts amd lavas) within these siltstones, Basic

dvkes cut the breccia and overlying sediments

m numerous localities.

Lithvlogy of Cottans Brecei

The breccia is jenerally a very poorly

gorted, crudely stratified mock wath angular

clasts sel in a carbonate, or a limenite, cement

(Fivs. (0, 1) and 12).

The breccia varies in thickness from about

40 nt inthe Rebhins Creek/ Cumberland Creek

are to abour 100 m in the City of Melbourne

Bay urea, However, in the City of Melbourne

Koy area Ihe out-crop is poor and the figure

of 100 m may he excessive. In the Cunglo-

merate Créeck urea between the mouth of Con-

plomerate Creek and Shower Droplet Rock

the thickness 1s about 80 m althaugh outerop

ig poor (Figs. 4 and 5) so that the exact thick-

ness is dificult ta obtain. However, the pre-

sence of scattered float in the parts of the sec-

lions Shown in Figs, 4 und 5 as “No utterop™

suggests that SO mr is the approximate thick-

ness of Cottons Breccia in the Conglomerate

Creck/Shower Droplet Rock ares. Thus, there

appears & definite thinning to the north. As

noted above, neither the top nur the hettom

of the breceia is exposed in the Cottons Flat

arcu south of City of Melbourne Bay.

The hrescia shows great lithological varia-

Gon, both lateral and vertical, over extremely

short distances. Fig, 5 shows the distribution

of elast sizes within the breccia frum various

seglions. ‘The fine breccia in Fig. 3 is where

few or to elpsts are over 10 em across,

melinm beceia is considered to be where

there are a substantial number of clasts be-

tween 10 snd 20 em across, but few abave 20

eit across: course breccia is considered to be

where there arc a substantial number of clasts

mute than 20 em across, Admittedly, this. ir

an arhitrary subdivision, but it was found to

be a convenient one in the field: hence ? feel

that it is of some value As shown in Fig. 5,

there is no correlation on the basis of clist

sive even in closely spaced sechons. However,

it the Conglomerate Creek/The Gut area there

is an apparently continuous, very coarse hori-

zon (1 to 4m thick} just below the top of the

breccia (Figs. 6, 7, 13 and 14). The breccia

it Robbins Creek, the northernmost section

measured, showed less variation in average

Mast size than ual the breccia further squth.

Thin Cup to 30 cm across and 10m lon),

comparatively well-sorted siltxtone afd sand-

sloiwe lenses are reasonably common within the

hrecein (Vigs. }Oand 15). Most horizons show

foie sighs of crude stratiivation with Jurger

clasts tending to line up with theis long axes

roughly purallel to the stratification (Pigs, 1]

and 15). Between Cottons Flat and The Gat

there is an apparently continuous hartéun wi

tuff which in thin. section shows shards.

The great majority of the clasts show some

rounding (Figs. 11 and 13) although some

show no roumling at all (Figs, 16 pnd 17}-

The largest clasts at any level are usually 30-

$0 em actress although at many bhomvons they

are less than 10 em across (My. 15)- How-

ever, at The Gut there is a 75 mi intervil of

very Jarve cream carbonate clasts wilh Lie

largest clast being over 3.3 m long, This large

boulder is itself a conglomerate with lyht prey

carbanate and chert clasts set in a ercam car-

honule (ies. 18 and 19), No similuc yery

larac clasts were seén away from Uhe Gut.

The clas! types include various carbonates,

ipiarizite, pyritic quartzite, chert, metasilt-

stones, sandstones, rect jasper and basic lavas,

The vartous carbonates: dominate the elast

assemblage with cream and grey dolomites

being the most common (Fig, 12), except in

the Cottons Plat area where quartzite clasts

tend to be as common as the carbunate clasis.

A very dark limestone is found occasionally

near the top of the breccia (Fig. 13); # [ew

oolitic limestone clasts are known throughout

the sections.

Quurizite clasts tend to make up the

majority of clasts uver 20 cm across, The

pyrilic quartzite clasts were seen only in the

Cottons Flat area. The smallest clasts (less

(han 3 om) tend ta conlain a predominance of

black, greet and grey. sometimes laminated,

metasiltstones, Rare cross-bedded — siltstone

clasts are known, The red jasper clasts ate

quite rare, although they are up to 40 cm

across.

Tit any one section, a particular cream dolo-

mite or a black metasiltstane may predominite

at a vertaia level, However, when plotted over

the whale ared. it was found that the commen

clast types occur throughout the breccia and

thar no particular clust type can be sotd to he

characteristic of any particular level within the

breccia, with the probable exception of the rare

very dark limestone mentioned ahove.

Very rare clasts of basic Invas ure known.

No acid igneous rocks of high grade metamor-

CIA, KING ISLAND, TASMANIA

OTTONS BREC

THE ORIGIN OF

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LHE ORIGIN OF OOTTONS BRECCIA, KING ISLAND, TASMANIA 21

phi: recks are known from the clast assem-=

blage.

Since the source of the clasts is inknown, a

classification into intrabasinal and extrubasinal

lypes in the manner of Schermerhorn & Stan-

ton (1963) is inapplicable,

Sedimentary Structures within the Breccia

In the Cottons Flat area, graded bedding is

quite conimon, There are two scales of graded

hedding, The finer scale of graded bodding is

exposed towards the base of the outerops in a

fine green sandstone and siltstone with pyrite

pseudomerphs, Each graded layer is between

2 and 7 em across. The best exposures of the

coarser scale of graded bedding are Just south

of Cottons Creek where each graded Jayer is

up to 30 ¢m across (Fig. 20). One possible

example of reversed grading is scen in the

Cartons Flat jrea, Graded bedding as not seen

awpy [rom the southerit outcrops,

There is af lenst one well marked local dis-

conformily within the hraccia at (be southern-

most oulcrop at Cottons Plat. There appear to

he disconformities within the breccia at ather

Iocaliuies, cg, at The Gut just abave the

biggest clast (Fig. 21). However, the generally

very poorly bedded pature of the breccia

makes disvonformities within it difficult to. pick

out,

There tre a few examples of wet sedinicit

movement within the breceiw. At one Inoation

in the Cottons Flat area convolnted bediiny

iidicates 4 west to east muvemeni of the scdi-

ment, In the vicinity af The Gut there ure

rare clasts af sandstone Which show lear evi-

dence of being transported lo the site nf ue

position before hein properly consolidated

(Fig. 22),

Striated pebbles have been feparted by Solo-

mon (1969), but the weiter did nov observe

any Such pebbles. Theee are several examples

of what may be drop-siones (Pigs. 23 ans 24},

These figures show possible drop-stones in the

Cottons Flat area, Figure 24 is of particular

interest tr dhat the surrounding sediment is

reasonably fine grained. About 5 cry below at

there is a 6 cm thick set of Jamimae of graded

fine sandstones and siltstones which could be

interpreted as yarves.

Origin of Cottons Breecia

The criteria used for the recognition of

glacial sediments have been discussed or listed

by several workers (Flint 1961, 1971, Harland

1964, 1963, SchWarvbach 1964: Heeven &

Hollister 1964; Harland er al, 1966: Hamilran

& Krnsley 1967; Kroner & Rankama 1972).

Harland e af (1966) comprehensively

reviewed the criteria for distinguishing lillites

from other rocks, They concluded that there

is Only one criterion which con be considered

lo be unequivocally in favour of a sediment

having a elavial origin, ie the presence of

uumerous large boulders penetrating and de-

forming a series of host strata. However, as

noted by Harland et al. (1966) the shape,

surface, size and composition of the clasts

within the sediment under consideration may

be used in favour of a glacial origin if the

features are of sutlivient quantity and quality.

Harland er af. (1966) also note that the

presence of extensive grooved and striated

pavements also clearly indicates glacial abra-

sion, e.g. the Lite Precambrian pavements of

the Kimberly Revion of Western Australia des-

cribed and figured) by Dow (1965), Dow &

Gemuts (1969) and Perry & Roberts (1968),

However, problems arise when there ave only

limited exposures: of pavements or possible

pavements (¢.2, Daily vf al, 19735. One af the

most commonly used criteria lor evidence of

glaciation is the presence of striated clasts,

However, striations can be formed by other

menns (Harland ef af, 1966). Despite this,

some workers (e.g. Bruckner & Anderson

[971) continue te use the presence of! striated

clasts as unequivocal evidence of a stacial

origin for the enclosing sediment.

Tf a tillite-like sediment is not of vlaciogeric

origin, the most commonly postulated alterna-

tive explanation is a mudtiow or density flaw

Origin (eg. Schermerhom & Stanton 1963;

Winlerer 1964; Schermerhorn 1964), Scher-

merhorn & Stanton (1963) listed 22 points as

evidence in determining whether « breccia

from the West Congn Gieasyncline should be

considered to be of glacial origin ur of density

Raw origin, Kifhurn ey al, (£965, p, 358) dts

pulte the validity of all but three of these cri-

letig and suggest that the criteria which favour

a density flow origin are (1) the presence of

graded bedding, (2) the presence of the largest

boulders in the thickest tillite-like beds and (3)

the occurrence of tillite-like sediments at the

beginning of sedimentary cyeles accompanied

by sharp epeirogenic downwarping of the

basin. Flint (1971, Table 7-B) tabulated the

characterrstics of tills and tillites ss compared

with fllite-like sediments of non-glaciogenic

nrigin. Heezen & Hollister (1964) stated that

turbidity current deposits are frequently

associated with glaciation but thay need not

he An example of this is the Lute Palaeozoic

glacial sequences af the Falkland Islands which

2 | B. JAGO

in purt dre the result of submarine mass moye-

ment {Frakes & Crowell 1967) allhough a

similar tase from the Late Precambrian of

northern Nopyay desuribed by Siedlecka &

Roberts (1972) has been strongly disputed by

Bjonykke (19733, Heeven & Hollister (1964,

Table 1) suggested (hal although turbidity cur-

rent deposits tre clearly different from placio-

veme sediments, lillites and sediments of mud-

flow origin ure very difficult to distinguash.

Kilburn et al (1965) and Spencer (1971)

have suggested that the presence of discon-

tinuwas horizons of sorted sediment (mudstonc

and sandstone) within structureless breccia

are dificult io explain by a mudflow hypothesis

und that such horizons indicate a glacial origin

for the breceit, Dott (1963), Fisher (1971)

und Cook er al, (1972) have discussed various

uspeets of sediments derived from submarine

eravity transport,

The pomls in favour of Cottons Breccia

being of glaciogenic origin are

(1) the angular nature of most clasts:

(2) the passihility of drap-stones being

present,

(3) the presence ot some fine graded sedi-

ments within the breccia in the Cottons

Mlat area which could be interpreted as

varves;

(4) the prescnee of undetarmed and com-

paratively well sorted sandstone and

siltstone Lenses up to 10 om long within

the breccia.

The maim Featires of the rock suggesting

that the rock is oot of ginciogenic origin are;

(1) The presence of a considerable amount

of coarse graded bedding in the Cottons

Ilal area, Although the fine seule grad-

ing noted above could be considered

as varves, the coarse grading shown in

Fig. 20 is unlikely to have been de-

posited hy wlacial action.

(2) She “conglomerate in conglomerate”

nature ol the furgest boulder at ‘The

Gut indicating that there are at least

Iwo similar depositional cycles involved

in the deposition of this boulder.

(3) ‘The only non-sedimentary clast types

are rare basic Javas which are alniost

certainly of local origin. In other well

known placial sequences, e.g, the Per-

mian rocks of Tasmania and the Late

Precambrian Sturt Tillite of South Aus-

tralia, metamorphic and igneous clasts

are yery promment where there are

abuudant wlasts. This suggests a oit-

glacial origin lor Cottons Breccia,

although such evidence is clearly far

from conclusive, because the clast types

in glacial sequences depend on the ter-

rain over which a glacier has passed.

No formation similar to Cottons Breeei is

known in the Late Precumbnan or Cambrian

sequences of Tasmania: If such i formetion

was found in a similar stratigraphic position

then the acrial extent of the rock woyld

probably indicate a glacial origi.

Dolomite, or a dolomitic siltstone. 15 closely

associated with many of the confirmed Austra-

lian Late Precambrian tillites (Dunn et of.

1971). Spencer (1971) and Spencer & Spencer

(1972) have noted the association of proven

tillites and dolumites in Late Precambnan

sequences, The presence of dolomite and dolo-

miti¢ siltstones just above Cottons Brescia May

indicate glacial or at leust cold conditions,

Speneer & Spencer (1972) have moled the

appuirent contradittion of the high temperature

origin (>22°C or 35-S55°C) usually propused

lor primary dolomile in relation to the

ussoviated cold temperature tillites.

Fisher (1971) has suggested (hut course.

grained deposits, forrned by high concentration

debris flows. will be poorly sorted, will have

un utwupperted framework, may include elon-

pute frauments aligned roughly partllel with

the hedding and may show inverse erading.

These features are present in Cottons Hreveta

except that the grading in Cottons Brevela ts

normal, However, as nated above, sediments

furmed by submarine mass movernent are

guile likely to be found in a ghicral enviran-

ment.

The presence of volcanics within Cottons

Brescia indicates thal, at the time of deposi

tion, the King Island area may have been tee-

tonically active. Intermittent earthyuakes vould

have given rise to a series of Uchbris flows.

Against this is the presenee of the contpara-

tively well sorted thin lenses of sinustone und

siltstone within the breeeia. Such bodies are

dificult to explain if a gravily slide mechanism

is invoked for the origin of the breccia {Kil-

burn ef al, 1965; Spencer 1971).

Conclusions

The evidence discussed above docs not pro-

vide an unequivocal answer to the problem of

the origin of Cottons Breccia, Features such as

drop-slanes, the thin sandstone lenses within

the breccia and the associated dolamite favour

w glacial origin. The presence of graded bed-

ding, the crudely stratified nature ol the breccia

and the faet thar almost all the clasts are of

THE ORIGIN OF COTTONS BRECCIA, KING ISLAND, TASMANLA 33

sedimentury origin tend to favuur yw density

flow formation. It ts possible that Cuttons

Breccia originated in a tectonically active area

by a combination of glacial action and sub-

mutine mass transport, Le. it May represent a

density flow deposit derived from an area

affected hy glaciation. The area in which the

breccia was deposited was intermittently alfec-

ted by volcanism and may have had twebergs

floating on the overlying sea, releasing debris

which dropped into the underlying sediment.

Acknowledgements

Thus work would not have been possible

without u grant from the Keyl Society of

South Australia Research and Endowment

Fund, Mr. M. Rogers, Senior Geologist ul

Geopeku Limited, kindly arranged accammo-

dation at Grassy; he generously supplied the

writer wilh maps and sections of the areca,

Mr. J, Skipworth of City of Melbourne Bay

kindly allowed the writer access to the out-

craps worth and south of City of Melburene

Bay. Mr. D. Carver and Miss A. Boos pro-

vided villuuble technical assistance. Dr. A. S.

Joyce (South Austrajian Institute al Tech-

nology) em Uhanked for advicy on thin section

work, Dr B. Daily (University of Adelaide)

gave valuable advice.

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o4 J. B, JAGO

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Unit, Univ. Cape Town, Bull, 11.

Larce, R, R. (1971) —Metasomatism and schee-

lite mineralization at Bold Head, King Island.

Prov. Aust. Min. Met. 238, 31-45,

McDoucart, I., & Leaso, P. J. (19645).—Isoiopic

age determinations on granitic rocks from

Tasmania. J. geol, Soe. Aust. 12, 295-332.

Perry, W. J., & Rowerts, H, G. (1968),—Late

Precambrian Glaciated Pavements in the

Kimberley Region, Western Australia. J. geal.

Soc. Aust. 15, 51-56,

RANKAMA, K. (1973).—A note on ile terminology

of ancient glaciogenic and similar nonglacio-

genic sedimentary rocks and on their nse in

formal stratigraphic nomenclature. Quart.

geal. Notes, geol, Surv. NSW, 13, 4-5,

Scurreurernoarn, L. J. G. (1966)—Terminology

of mixed coarse-fine sediments. J. Sed, Pct,

36, 831-835.

SCHERMERHORN. L. J. G, & Sranton, W. L,

(1963),-—Tilloids in the West Congo. Geo-

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ScrwarzpacH, M. (1964)—Crileria for the

recognition of ancient glaciations. Jn A. E. M.

Nairn (Ed.), “Problems in FPalaeo-

climatology”, pp. 81-85, 110. (Interscience:

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Scxuwarzpacn, M. (1965)—Palaoklimatologische

Eindriicke aus Australien nebst einigen allge-

meinen Bemerkungen zur dlteren Klima-

Salt ag der Erde. Geol. Rundschauu 54,

128-160.

Stspiecea, Ay, & Rosertrs, D. (1972).—A Late

Precambrian tilloid from Varangerhalvoya—

evidence of both glaciation and subaqueous

mass movement. Norsk. geol. tidsskr. 52, 135-

141,

Scott, B. (1951).—The Petrology of the Vol-

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mania. Pap. Proc. R. Soc. Tasm. (1950),

113-136.

Smira, E, M., & Wirtzams, E. (Eds.) (1965).—

Geological Excursions for the. Australian and

Wew Zealand Association for the Advance-

ment of Science, Thirty-Eighth Congress,

Depi. Min. Tasm.

Solomon, M. (1969).—The nature and possible

origin of the pillow lavas and hyaloclastic

breccias of King Island, Australia. Q, J. geol.

Soe. Lond. 124, (53-169.

Spencer, A. M. (1971). —Late Pre-Cambrian

Glaciation in Scotland. Mein. geol. Soc, Lond.

Srencer, A, M., & Spencer, M. O. (1972).—The

Late Precambrian/Lower Cambrian Bona-

haven Dolomite of Islay and its stromatolites.

Scott. J. Geol. 8, 269-282.

Spry, A. H. (195%)—Some obscrvations of the

Surassic dolerite of the Eureka Cone Sheet,

near Zeehan, Tasmania. Jn “Dolerite—A

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Hobart.)

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“The Geology of Tasmania”. J. geol. Sac.

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Watrroouse, TL. L. (1916).—Notes on Geology

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Win tereR, BE. LL. (1964).—Late Precambrian

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‘Problems in Paluecclimatology”, pp, 159-

178, 186-187. (Interscience: New York.)

J. B. JAGO

Figs. 6-13

Figs

Fig.

J.B. IAGO

6.7. Conformable contact between Cottons Brecci and the overlying laminated haenatitic sand-

Ih.

iw. V4,

19.

stone and siltstone. In Fig. 6 nole the Juminated nature of the overlying haematitic sand-

stone and siltstone. Locality, immediately north of The Gut. Hammer Jength is 32.5 em,

Disconformuble contact between Cottons Breccia und the overlying dolomilic siltstone. Pen-

cil points to the contact. Note the pebbly nature of the base of the dolomitic siltstone and

itis more luminated nature higher in the section. Locality, about LOO m south of Shower

Droplet Rock, Hammer length, 32,5 em,

Disconformable contact between Cottons Breeeia and the overlying dolomitic silistone. Pen-

cil points to the contact. Note the very pebbly nature of the base of the dolomitic siltstone.

Locality, close to that of Fie. 8 Pence Jeneth, 15 em.

Sundstone lens within Cottons Breccin. Locality, aboul 40 m south of the mouth of Cottons

Creck. Hammer length, 32.5 cm.

Long axes of clasts uligned roughly parallel to the strutiication. Locality near Shower Drap

let rock. The largest pebble is about 15 em long.

Vine breccia showing pockmarked nature of rock due to carbonate pebbles being eroded oul

Locality, The Gut. Hammer length, 32.5 cm,

Very course breccit neur lop of Cottons Brecein, Note the slightly rounded nature of almost

all clasts. The four large very dark clasts, including: the one immediately below the hammer

head, are composed of a dark limestone which is found only near the top of the formation

Most of the larger pebbles pre quartzite, Locality, The Gut Hammer Length, 32.5 cm,

Very coarse horizon near top of Coulons Breccia, Note the overlying guile fine heron.

Locality, Section NB about 100 m north of Conglomerate Creek, Hammer length, 32.3 em.

Silistone lens wilhin Cottons Breccia, Note the alignment with bedding of the large carbonate

boulder to the right of the hammer. Locality, The Crat. Hammer length, 32.5 em.

Lurge (lat clast (quartzite) showing vo sign of rounding, Locality. section C-D, Hammer

Jeneth, 32.5 cm,

Lurge angular clast (quartaite), Locality, Cottons Flat. Hammer length, 32.5 cm,

Very large carbonate clast (otal length is at least 3.3 m). Note the conglomeratic nature of

the clist which contains light grey carbonate and chert clasts 1p to 12 em across. Locality,

The Gut. Hammer length, 32.5 em.

Same chist as in Pig. 18. The top and bottom of this large clast are roughly parallel with

the bedding which trends from the top left lo the bollom right olf the photograph, Hummer

length, 32.5 cm,

Course vraded bedding on broken slab of breeen. Locality. 30 m south of mouth of Cottons

Creek. Hammer length 32,5 om.

Possible disconformity (lip of pencil) within Cottons Breceit. Largest clast (see Figs, 18 and

19) is immediately below the field of view. Locality, The Cul. Hammer length, 32.5 em,

Sondstone clast showing disturbed bedding indicating Ahat i wits Leanmsparted to the site of

deposition before jt was properly consolidated, Locality, the Gut. Hammer length, 32.5 en

Possible drop-stone. Locality, Cottons Flat. Pencil length, 14 em.

Possitle drop-stone. Note the laminated and graded mature of the fine sandstone and siltstone

a short distance below the (?) drop-stone. These could be interpreted as varves, Locality,

Cottons Flat. Pencil length, 15 em.

Fine breceta. Locality, about half way between the mouth of (he Conglomerate Creek and

Shower Droplet Rock. Pencil length, 15 em.

THE

ORIGIN OF COTTONS BRECCIA, KING ISLAND. TASMANIA

STRATIGRAPHY AND PALYNOLOGY OF THE PERMIAN AT

WATERLOO BAY, YORKE PENINSULA, SOUTH AUSTRALIA

BY C. B. FOSTER*

Summary

FOSTER, C. B. ( 1 974) .-Stratigraphy and palynology of the Permian at Waterloo Bay, Yorke

Peninsula, South Australia. Trans. R. Soc. S. Aust. 98(1), 29-42, 28 February, 1974.

The discovery of Permian and reworked Devonian microfloras in glacigene sediments from the

Troubridge Basin led to a detailed study of the stratigraphy and palynology of the Waterloo Bay

area. Quantitative palynological analyses indicate one microfloral assemblage which is equated with

Evans' (1969) "Stage" 2 microflora and is of Early Permian age. As a result these sediments have

been correlated with other Permian deposits in southern, eastern and western Australia. A biofacies

study indicates a low salinity palaeoenvironment which most probably resulted from deglaciation

coinciding with a marine transgression that was affecting Southern Australia at this time.

STRATIGRAPHY AND PALYNOLOGY OF THE PERMIAN AT WATERLOO BAY,

YORKE PENINSULA, SOUTH AUSTRALIA

by C, B, Postir*

Summary

bosrer, C.. B.. (1974).—Stratigraphy and palynology of the Permian ai Waterloo Bay, Yurke

Peninsula, South Australia. Trans. R. Soc. S.-Aust, 98(1), 29-42, 28 February, 1974.

The discovery of Permian and reworked Devonian microfloras in glucigene sediments

from the Troubridge Basin Jed to a detailed study of the stratigraphy and palynulogy of the

Waterloo Bay area. Quantitative palynological analyses indicate one microfioral assemblage

which is equated with Evans’ (1969) “Stage” 2 microflora and is of Karly Permian uge. As

w result thess sediments have been correlated with other Permian dcpasits in southern, eaastey'n

and western Australia. A biofacies study indicates @ low salinity palaeoenyironment which

most probably resulted from deglaciation coimciding with a marine transpressian that wus

udlecting Southern Anstralia at this time.

Introduction

Palynostratigraphic corrclations with other

Permisn deposils of Australia have resulted

from the resovery of Permian, and reworked

Devonian, miospores from sediments of the

Waterloo Bay area (Fig. 2). The sediments of

the Troubridge Basin are regarded as glacigene

deposits (Ludbrook 1969a)-_ Field observations

and » biofacies analysis presented io this paper

support this and the consequent overall palaeo-

veographic setting.

The first record of a Permian microflora

within the Troubridge Basin (Fig. 1) was given

by Cookson (1955, p. 57) when she reported

reworked palynomorphs in a deposit of

“probable Eocene age", More recently, Harris

& McGowran (1971) recorded for the first

time in situ Permian miospores. One sample

collected from the Waterloo Bay area yielded a

particularly well preserved assemblage. The

purpose of this study was to re-examine the

section containing this assemblage. This in-

volved detailed mapping and precise strati-

graphis sampling. Samples collected yielded

palynomorphs and Foraminifera; no other

fossil groups were found. Subsurface material

from the Peesey Swamp bore, PDH No. |,

provided moderately well preserved assem-

blages allowing an intrabasinal correlation, This

Wis in contrast to the subsurface material

examined by Hartis & McGowran which was

poorly preserved, Bore locations are shown in

Fig. 1.

Methods

Clif! sections were measured using a

Jacoh staff with a sighting attachment

(Kottlowski 1965). Working from the water's

cdge, it was possible using Tide Tables

(S.A. Dept. Marine & Harbours 1972) to cal-

culate the height of the base of the cliff sec-

tions above mean sea Jevel. This provided the

“datum” shown in Fig. 2. Section locations.

were plotted on a base map prepared from air

photographs (S.A. Dept. Lands, Svy.962:

2549, 2535) and section heights checked with

the Edithburgh Topographic Map (Sheet 828:

S.A. Dept. Lands). A 7 cm diameter “post

hole digger” was used for field sampling to

obtain Iess weathered samples at depth (max.

1.2m).

Palynological samples were prepared by

treatment with hydrofluoric acid to remove

silicates. Excess organic material was then re-

moved using warm Schulze solution followed

hy alkali. The use of heavy liquid density

separations (ZaBr,; $.G. 1.98-1.6) and ultra-

sonic cleaning improved the yield, Sarnples

* Department of Geology and Mineralogy, University of Queensland, St. Tascia, Qld 4067.

30) C, B. FOSTER

examined for Foraminifera were processed

using standard techniques (Glaessner 1945).

Palynological residues and strew slides

deposited in the South Australian Geological

Survey Palynological Collection are prefixed

“§S". Slide coordinates given are from a Leitz

LOCALITY MAP

Laborlux microscope No. 579756 housed at

the Survey.

Locality

The study area, 16 km SW of Edithburgh,

occurs as upthrown fault blocks (Wopfner

1970) and forms the southwestern part of the

DENMAN

BAS I N

RENMARK

rnb

area _

LEGEND

m ADELAIDE 2 Permian Basin

Troubridge Shea)

Na.1

Waterloo Bay

KANGAROO ISLAND

Profile Locality

(See Fig.2)

Bore Hole

CBF |9VG

Fig. 1. Locality map.

PERMIAN SEQUENCE

Troubridge Basin, ax defined by Wopfoer

(19A9), It is gently wadulaling with salt lakes

occupying many of the low lying sreas. The

existence of these lakes, many with scattered

ertatics abuul their margins (Howchin 1900},

uifers the ubiquity ot the underlying Permian

clays. A thick calcrete capping obscures the

geology of the area except in coastal sections

where maximum thicknesses of 31 m are ex-

posed. Large e¢rrutics and boulder trains litter

touch of the beach area, Pink garnetiferous

sands, Which have been associated with glaci-

gene deposits (Coats 1962), occur in high con

venttations along parts of the beach.

Stratigraphy

Columnar stratigraphic sections and the

coastal profile of Waterloo Bay are shown in

Fig, 2.

Permian

The lowermost outcrop, a brown gritty silt-

stohe containing erratics, occurs 4t beach level

and is poorly exposed, Small-scale slimp strne-

tures Were observed, although elsewhere there

is no evidence of bedding. Samples collected

from thts level were barren,

Overlying this, and forming the base of the

cliff sections, are black to blue-grey, sandy,

micaceous clays. They are carbonaceous in part

and on weuthering appear grey-white. The sand

fraction is poorly sorted jd ranees from elear,

angular to frosted, well rounded grains, Maxi-

mum thickness of the unit is 12 m. Small

erratics (3 cm?) of granitic, pneissic and

quartvose composilion are scattered through-

out. These are smaller than the erratics on the

heach, which have heen reworked to form

modern lag deposits. The sediments are

moderately tndurated, but lack the fissility

typical of shales and the compactness of mud-

stones; consequently they are referred to as

claystones (Pettijohn 1957). Samples yielded a

well prescrved microflora und a few arenaccaus

Foraminifera,

Interbedded withm the claystanes are dis-

continuous sand lenses, which jnclude fine

Srained light blue to white and coarse red

sands. The origin of these sands is not known,

allhough RK. P. Hazris (1971, unpublished BSc.

Honours Thesis, University of Adelaide} has

suggested that they are wind blown. Samples

colected from these lenses for foraminiferal

analysis were barren, Many of the lenses

exhibit prominent ferruginous concretionaty

structures, up to 1 m im diameters these are

mest probably weathering features. Generally

AT WATERIOO KAY al

thy contact betWeen the claystones and the

sand is sharp; al one locality (Section 3, Fig,

2). Uw lens overlics @ cobble bed (40 cm

Ihick} but it 1s nol traceable for more than 2

in. The bed could represent Permian reworked

sediments forming 1 channel deposit. Similar

lag deposits were seen af Point Turton (Fig.

1),

Much of the unit is severely ironstdined

which gives the outcrop a grey/orange mottled

appearance, This appuareni lateritization

(Crawford 1965) could be a post-Permian sur-

face feature, Ludbrook (1965), however,

records iron-staining in subsutface material.

Reynolds & Johnson (1972) have reported

chemical weathering (iateritization) in a recent

subglacial environment, and so the possibility

oP this being a Permian feature caunnt be dis-

counted.

A comparison of the outcrop With the

lithologies. logged fromy the Stanshury No, 1

and Minlaton No. ? Stratigraphic bares (Lud-

rank 1965) places the claystones high within

the focal Permian section and inetudes them

within the Cape Jervis Beds (sce also Lud-

brook 196%b).

PPermiant Clays ana Sandstones

Clays, which are mottled reddish green,

occur mamly as slope cover. The heavily

weathered nature of the unit obscures tly houn-

dary contacts (max. thickness 5 m).

Sandstones, which consist of grey white, ill-

sorted, poorly todurated clayey sand with small

erratics. Where it is not in direct Contact with

the sca (eg. Section 8), it weathers to form

peculiar columnar structures. These appear to

be the result of two sets of “jointing”, the

earlicr horizontal set could be following bed-

ding planes with the latter set perpendicular to

the first. Maximum thickness 4 m.

Samples collected from these units were

barren and considering the possibility of post-

Permian reworking their exact age is nol

known. An essentially similar outcrop io that

of Scction 8 was found at Port Mocrowie

{Sections 2 and 3) and has been mapped as

“Pernuan” by Crawford (19651,

Tertiary

These ace horizontally bedded, buff to pink,

polyzoal limestones (Section 10) that have

been sporadically calcreted, They form resis-

tant headlands for 2 km along the coast to

Tronbndge Hill. Underlying the calerete the

pinkish limestone is strongly recrystallised and

shows numerous irregular solution cavities.

Below this level the mit becomes 1ess recrystal-

32 Cc, B. FOSTER

lied and contains distinclive butt coloured

“eub-units", Angular quartz gravel hands grad.

my upwards to coarse brown iron-stained sands

occur ol several intervals throughout the unit

Maxiutom thickness 24 m.

Foraminifera from samples. of these less in-

durated sub-inils indicate a Late Eocene aye

and suegest correlation with Rogue Furmation

und hasal Port Willunga Beds (J. M. Lindsay,

1972, SA Depariment of Mines, unpublished

report, RB 72/190).

The Pliocene Hallet Cove Limestone, which

Crawford (1965) has shown to occur at Point

Gilbert, was not found at this locality.

Ardrossan Clave and Sanedrock

1965)

The maximum thickness of Lhe unit at this

locality a8 1.7 m. This includes the mogrtled

green-brown sandy clays containing grit bands

and deeply weathered erratics pnd the uncon-

formably overlying red-brown clays with their

distinctive “alunite snd/or kaolinite’ hands

(Crawford 1965, pp. 40-41).

X-ray diffracymeter (X.R.D.) analysis of

samples collected from these bigds indicated

muinly ile (A. J. Love, personal communica-

tion). A similar lithology was saunypled at the

Tertiary/ Permian contact (Section 10) and

XRD. analysis showed a similat clay

mineralozy lo thar from the Quaternary

sequence, Therefore, it is most likely ihut these

bands are a post-deposttional feature

Cuaternary Acolianite and Calcrete

Acolianite, the maximum exposure of this

gecy-white poorly indurated calcarenite (§ m1),

oceurs where if Lorins 2 prominent headland and

an assuciated wave-cut platform (Section 5,

Fig, 2}. This is the only section which exhibits

lurge seule eross-bedding, Elsewhere in the pro-

file the until ts horizontally bedded but is easily

identified by its distinctive “swallow hole”

weathering pattern. Pladktonic and benthonic

Feraminifera reeavered by Lindsay (1972,

cited ahove) From a well bedded buff cal-

carenite (1 m thick) containcd within the

veolinnite sequence (Section 5) were con-

sidered by Lindsay to indicate 9 Late Cainozor

age and identification as Bridgewater Forma-

uon (Firman 1969),

Calerete, of varying thickness (ap to 8 m),

and in part underlying the aeolianite, farms a

blankeling surface seen in all sections. In

places it was possible to identify up to jive

distinctive “beds” which were of limited lateral

extent. One such “bed” (0.8 m, Section 3)

consisting of black, rounded to angular Frag-

(Crawtord

ments within a light green calcareous matrix,

could be traced for 10 m before becoming

“absorbed” inte the more missive featureless

galcrete 10 the east and faulted out to the west.

The unit is sandy and friable at the base

becoming more nodular to massive at the lop.

Taxonomic List of Permian Microflara

Forty-six species, from thirty genera, of

Permian palynomorphs were identified front ten

samples, Sample locations not shown on Fig,

Z occur away from the sections illustrated.

Precise locations of all samples accompany the

slides deposited at the Geological Survey.

Fifty-two strew slides were examined; selected

species are figured. The miospore genera are

arranged alphabetically within the classificatory

seheme proposed by Potonié (1956 aind subse-

quent publications) and its emendations,

especially those of Dettmann (1963).

Where necessary, brief notes on taxa have

been included: the descriptive terminology used

is in keeping with Kremp (1965). Disaccate

measurements are in accord with Segroves

(1969, Fig. |, p. 176).

Quuntitative microfioral dula and = the

chronostratigruphic significance of ihe Water-

low Bay Assemblage are discussed liter tn the

paper.

Anicturma SPORITES H, Potunié 1893

Turma MONOLETES Ibrahim 1933

Suprasublurma AcaVATOMONOLETES Dettmann

1963

Subturma AZONOMONOLETES Luber 1935

Laevigatosporites. flexas Segroves 170 (Fix.

14)

Leevigatosporiles sp.

Tubercalatosporites miodiens Ralmne & Hen-

nelly 1956

Turma TRILETES Reinsch, emend. Betiniain

1963

Suprasubturma AcavaTrTRieTRSs = Deltmnalin

L963

Subturma AZONOUTRILEDES Lube, cmend.

Dettmann 1963

Acunthoniletes terctianuwatuy Balwe & Hen-

nelly 1956

Apiculatisnoris levis

Segroves 1970

Apiculativporis sp. (Fig. 8)

Trilete, laesurae edtending to equator and

sometimes bifurcatmg at fermini. Lips

developed 0.5um wide and unseulptured. Amb

round to oval, boundary uneven. Spatsely

spaced hroad coni (1-2 ,m wide) are arranged

concentrically on the distal face. Diameter (10

specimens) 18-37 ym,

(Balme & tlennelty)

PERMIAN SEQUENCE AT WATERLOO BAY

‘ARG OOTIALEAA ‘A]JOId [elseO> pue suonoas oydei8ness reuUNOD *

SINT ONWS INZITY

54 Cc. B. FOSTER

Baculatisporites sp.

Calamaypora diversiformixs Balme & Hennelly

1956

Calaimospora sp. cf. C. microregosa Schopt,

Wilson & Bental! 1944

Deltaidespera directa (Balme & Hennelly)

Norris 1965

Densaisporites solids Segroves 1970

Granafatisporites sp. ct. G, teisinas Balme &

Hennelly 1956

Granwlatixsporites trisinus Balme & Hennelly

1956

Horriditriletes ramosuxy (Balme & Hennelly)

Bharadwaj & Salujha 1964

Krauselisporites sp.

Leschikisporis. cestus Segroves 1970

Laphorriletes sp. (Fig. 11}

Trilete, triangular amb with — strongly

developed concave sides, paralleling the

laesurue, Ruised lips (1 pm) slightly thickened,

Exine | pm thick supporting on the distal sur-

face and ul the equator small blunt cones (2

wm high, 1 ym apart) and spines 2-4 pm,

1.5 ,m apart. Ornament lacking on proximal

face. Diameter 35,.m. Differs from ¢f, L. versus

Bharadwaj & Salujha 1964 by the strong con-

cavity of the amb and the increased armament.

but lacks the thickened interradii ‘reas of C-

roviens Singh 1964,

Aficrohaculispora tentila Tiwari 1965

Punetaiiyporites. gretensiy Balme & Hennelly

1956

Prnctatisporites sp. cf. P. gretensis (Fig, 7)

In all regards this form resembles P, grefen-

sis, except in size. Av, diameter 20 pm cf, 118

ym. of the latter: The exine, 2 pm, 1 thicker

than that of P. rininius de Jersey 1960,

Verrucasisperites sp-

Antcturma POLLENITES R, Potonié 1931

Turma PLICATES Naumova 1939

Subturma MONOCOLPATES Iversen &

Trocls-Smith 195U

Cycadopites cymbatus (Balme & Hennelly)

Seygroves 1970

Marsupipollenites triradtatys forma iriradiatus

Balme & Hennelly 1956

TYurma SACCITES Erdiman 1947

Subturma MONOSACCITES Chitaley emend.

Potonié & Kremp 1954

Papasaccites gondwanensts (Balme & Hen-

nelly) Segroves 1969 (Fig. 16)

Purusaceites sp. A (Fig. 17)

Monosaccate, trilete scar ruptured on several

specimens. Distal saccus attachment overlaps

1/3 of corpus diameter, Amb triangular, with

undulant margin. Corpus rounded triangular in

shape. Sacci brochi clongate, 05-1 pm ia

diameter, Dimensions (3 specimens): T.D, 60

um, C.D. 30 ym. This species differs fram

lV. wriangularis (Mchta) Lele 1964 in that the

corpus is roundly triangular and not circular.

Parasaceites sp.

Parasaccites sp. cf, ¥, Mehtae Lele 1964

Parasaccites iiffusus Tiwari 1965

Potonieisporites: balmet (Hart) Segroves 1969

(Fig, 9)

!Moffmeisterties sp. (Fig. 19)

Monosaccate, Amb oval, corpus. sub-circu-

lar with marginal folds, Trilete mark not seen.

Saccus attachment. is equatorial and sub-

equatorial. Dimensions; longitudinal axis. 160

pm}; transverse axis 100 pm; corpus diameter

73 wm.

Subturma DISACCITES Cookson L947

Alisporites gracilis Segraves 1969

Limitispovites moersensis (Grebe)

1963 (Fig. 13)

Limitispariies sp. cf. L. reetus Leschik 1956

(Fig, 21)

Dillers from LZ. rectus being somewhat

larger; total breadth 76 ,.m, breadth of corpus

42 ym; saccus length 38 pm, corpus length 46

pm; cappa width 26 pm.

Protohaploxypinus rugatus Segroves 1969

Sviatoabietites multistriatus (Balme & Hen-

nelly) Hart 1965 (Fig. 5}

Sulcatisporites sp.

Sulcatisporites sp. cl, §. splendens Leschik

1956 (Fig, 18)

Filiatina sp.

Klaus

Incertae Sedis

Group ACRITARCHA Evitt 1963

Subgroup ACANTHOMORPHITAE Dewnie

et af, 1963

?Baltisphacridiuar sp. (Fig. 12)

Micrhystridium spp.

Subgroup POLYGONOMORPINTAE Downic

et al, 1963

Veryhachinm spp. (Fig. 10)

Subgroup NETROMORPHITAE Downie er al.

1963

Lelofusa spp. (Fig. 15)

Algae

Borryococeus braunii Kiltzing 1849 (Fig, 6)

Composition of Palynological Assemblage

No significant quantitative changes in ntic-

spore composition were recorded from any of

the samples (see Fig. 3), Unfortunately,

spores {ron the upper samples in Peesey

Swamp Ne. |b (10.6 m5 m) were too pourly

PERMIAN SEQUENCE AT WATERLOO BAY 35

WATCRLOG BAY ASSEMBLAGE

S 2419

MEAN *%

WATERLOO BAY ASSEMBLAGE

Migevebueuidspera ASSEMBLAGE

SEGROVES (1970)

A&B PERTH BASIN

Cad WATERLOO BAY

1 “TOTAL” SPORES

2 MONOSACCATE POLLEN

3 (NON STRIATE) DISACCATE POLLEN

4 (STRIATITI) . i“

5 SPINOSE ACRITARCHS

& NON SPINOSE ACRITARCHS

7 MONOCOLPATE POLLEN

8 MONOLETE SPORES

TRILETE SPORES

Acnihotvidetes ASSEMBLAGE 3

SEGROVES (1970)

NOTE: 1. SEGROVES DID NOT INCLUDE GROUPS 7, 8 & 9

2. “TOTAL SPORES FROM THE SUMMATION OF 8 & 9

PERCENT OF TOTAL ASSEMBLAGE

Fig. 3. Quantitative comparison of microfloral assemblages.

if C. B. FOSTER

preserved io allow airy firmer conclusious other

than that the fssemblage is of Permian age,

Consequently, ouly one microflora] assemblage

is considered lo be preset,

This well preserved, moderately diverse

assemblage is dominated by monosaccate

pollen including Poeronteisperites baled and

FParasuccites spp. (av. 20%, max, 30%).

Monoculpaie pollen. Cvcadopites cyimbetis, 18

also abundant (S--10%) as ix the trilete spore

Micrabaculispora teatila (12%). Nonestriate

bisaceates form a minor element of the assem-

blive (3¢6) .and striate bisaccates are rare

(<1%). Four venera of spinose acritarchs

are presen! (up ta 13%) and include Mery-

hachitun. Miorhystridium, and Lelofusa. Per-

centages are bused on a total count of 1,600

apecimens,

Apart from these elements, a well preserved

reworked Middle to Laie Devenian microflora

(up ta 298} is present, including Gemninesprra

lerawata Balme, Corvelutivpure fromenvix

Balme & Hassell, and Avcrvaspora sp. Fungal

spores, algac, Botryacocrus braanti, and wood

fragments lotm 4 minor background element.

No megaspores were found.

Biosiraligraphy and Age

The Australian Permian = mierofloral

sequence has been subdivided into various

pulynastratigraphic zones, Evans (1969),

working in southern und eusterm Australia,

erected a five-fold subdivision (“Stages 1-5)

which he considered ranved from Late Car-

bonilerons through to Late Pennian (Stages

25). He related these Stugexs to the early

work by Balme (1964) in Wester Australia.

Paten (1969) re-subdivided Stages 45 into six

sub-stages on material from ihe Cooper Basin

(South Austeatia). More recently Scgraves

(1970) produced five assemblage zones within

the Permian sequence of the Perth Basin. The

relalionship hetween these schemes is shown

in Fig. 4. Atthouwh the late Karly to Late Per-

minh subdivisions do not apply ia this study,

they have heen included for completeness

Recugnition of these subdivisions is based

upon the first appearances of key specics and

the quantitative composition of the assembluge

(in particular Segroves 1970; this study). Prob-

lems exist using this approach because of

facies variuliums (Balme 1969; sec later), and

ih Many cases the precise stratigraphic ranges

of the key species are not known Negative

evidence such as [he absence of a particular

Stave (indicator within a well preserved assem-

lage is often used to preclude it Frans heing

younger than that Stage. This approach may

noc be desirable and it reflects the need for

further study of the Austealian Permian, The

writer iy currently engaged in research into

these problems in the Bowen Basin, central

Queensland.

Coarrelation

The Waterloo Bay Assemblage muy be com-

pared with Evans’ (1969) assomblages

(‘Stages’) and with those of Segroves (1970)-

The correlation usmg both works is shown

separately and the differences are discussed.

Two species, Deltoiduspora directa and

Maérsepipofenties triradiutus forma, triradiatis,

which Evans (1969, Vig. 4) has shown do hor

oveur in ussembliuges older than his Stage 2.

were found in the Waterloo Ray Assemblage.

In addition the presence of striate bisaccate

forms. c.g, Proloheploxsypinus rugatus, exclude

the assemblage from Stage 1, The absence of

Fermneavisperites psreudoreticulats, a. Stage 3

index form, within this well-preserved assem-

blage, is taken Lo indicate that the microflora

ts nul younger than Stage 2, Consequently,

using these criteria (he Walerloao Bay Assem-

blage i& equated with Stage 2,

In terms of Segroves’ units (L970, text. fix.

2) the Waterloo Bay Assemblage compures

closely with that of the “Micrabaculispora

Assemblage" (Stage 2, Evans’ units). A quanti-

tative comparison is given in Fig. 3 The

slightly higher percentage of striate bisuceale

pollen at Waterloo Bay suggests that its micro-

fiora is younger than the Perth Basin assem-

htage, and is therefore correlated with the

upper Nangelly Vormatian, Perth Basm.

However. using the range chart (Seeroves

1970, fig, 4) the Waterloo Bay Assemblave

appears ta correlate with the “deanthetrileres

Assemblage” (Stage 3 plus lower Stage 4;

bvans" units). ‘The species whose ranges indi-

cafe this are Grannlatisporites trisinus, Tuber-

culctosporites modicus and Laevivatosporites

flexuy; and are included with several other

species (yiz. C. diversiformits, .4. teretiangu-

fatus, A. levis) of the ien considered diagnos-

tic of that assemblage (Scgroves 1970, p. 514).

‘Yo check this discrepancy the two microfloras

were compared quantitatively (Fig, 3). The

Waterloo Bay Assemblage way found to differ

from the “Acanthetriferes Assemblage’ as

tollows:

(i) The greater abundance of monosaccute

pollen,

PERMIAN SEQUENCE AT WATERLOO BAY 47

PLATE CARBON IFEROUS EARLY PERMIAN PLATC PERMIAN

MMarobactiispom: | duadyienorites | Aeaitho. Fp Linsye tia Pulfimeleeepors Assemblage

QL6T

SANG

Assemblage Assems}age Assam] aye

a3emb]sge ; oe iydhur ony ASspmhlage

SANOZ TWeO140Y liv

Assetblage Toga bettie Pe Assemblage.

* andi uaddn

SdTYenoul

}

aLBul | tueg

RAUEMBUL LY)

Pasemeun yey

SLEyS

aaust Any

‘Wy Uo [Lsdy

:]Pauasoy

‘W) Se4yb roo,

NISWS YF4d903

2191 asnoyazeg

GIDGEALPA FORMAT LON

io pow

‘

{

)

BUpAey UCN,

uoLirsudap

4X8) fas

TON BUsaoouezOOR

PUL plod,

NISVd VONTUVRdaY

Toon yues Appny

Siduey |y2l6i Shey

WUjod UMoug

226.

6961 Sh44eH

“qdaq yg sqvoday pays ..qndy

Sauly

Oot Shidey

Fig. 4. Permian microfloral subdivision, South Australian biostratigraphy.

4B CG. B, FOSTER

(ii) The greater abundance of spinose acri-

tarchs.

(li) The lower frequency of bisaccate

pollen,

‘The first two can be explamed by facies

variations, the acritarchs indicating saline con-

ditiahs, while the monosaccate pollen indicate

proximity to the floral source, as their disper-

sal is effected by wind and water currents

(Muller 1959). However, the low frequency

of bisaecatés cannot be explained by the same

reasoning, and is considered significant as they

reflect the progression of floral evolution

(Balme 1962). Consequently the apparent

correlation (ic. with the “Acanthatriletes As.

semhiave) is rejected. Because of this, the

stratigraphic ranges of these three species, mien-

tioned above, presumably extend into earlier

Permian strata,

age

Marine shelly fossils from the Nangetty For-

mation. Perth Basin, and the Upper Lochinvar

Formation, Sydney Basin, hoth Stage 2 micro-

floral localities, have been correlated with those:

from the type Sakmarian (Dickins 1963,

19682, b) and are accordingly of Karly Per-

mian age, The Waterloo Bay Assemblage cor-

telated herein with the Stage 2 microflora is.

therefore, of Early Permian age. Moreover the

gross microfforal composition of this assem-

blage, in particular the low percentage tacniate

hisaceate poilen, is considered indicative of

middle Sakmarinn age (Ralme 1962; Segroves

1969; Hart L971).

Although problems jn correlating the Aus-

tralian Permian with the standard Russian sec-

tions exist (see Waterhouse 1970), the

Standard Stage names ave used in this paper

to allow rapid comparisons with earlier pub-

lished works. However, should the recent con-

clusions of Balme (1973) regarding the posi-

tion of the Carboniferous/Permian boundary

he accepted, the Waterloo Bay Assemblave will

be of Late Carboniferous age.

Local Implications

Correlations with other Permian scdiments

within South Australia are shown in Fig. 4.

Such information is useful in palaeogeouraphic

and environmental interpretations, Within the

Troubridge Basin the outcrop at Waterloo Bay

has been correlated with at least 35 m of Per-

mian sediments intersected (45-80.5 m) in

Poesey Swamp No, |,

The high frequency of reworked, execl-

lently preserved Devonian spores suggests a

local origin (Harris & McGowran 1971), Long

distance transport along ice movement path-

ways [rom areas of proven Devonian sedimen-

tation (eg. Antarctica, Uclhy & McElroy

1969) would destroy the palynomorphs, par-

Licularly these with delicate appendages such

as Anervespora. This ts further evidence of

Devonian deposition within the State (see

Harris & McGowran 1973).

Faviranment

The following environmental inferences are

made [rom a consideration of the preserved

associations of microfossil groups in the Water-

foo Bay sediments.

Spinose acritarchs have in general been re-

garded ns indicators of marine conditions or

marine influences (Downie, Evitt & Sarjeani

1963), Smith & Saunders (1970, p. 324)

demonstrated that acyitarchs of the same

genera (viz, Feryhachiurm, Baltisphaeridium:

also see Staplin 1961) as those from Permian

sequences ate “confined to areas continuously

or intermittently open to marine waters and

FIGS, 5-21

All figures x 400,

Pig

Fig.

Fig. 7, Punctatisporites sp,

8. Apiculalixperis sp., S$ 2441/2, 27,8:110,1.

- Laphatriletes sp,, 8 2388/1, 48.0; 104.7,

Letojisa sp., 8 2389/1, 33,0:93.3.

5, Strintuahtetites, maltistriatus (Balme & Uenneliy) Hart, § 2267/3, 23,8:114.1.

6 Botrvococens Pbraunii Kitzing, S 2267/1, 25,5:113.0,

cf. P. erétensis Balme & Hennelly, & 2267/4. 40,8:101,9,

- Poronteisporires balmet (Hart) Segroves, S 23%)! 1, 32,3;99.8-

. Fervhachinm sp. (cluster), S 2267/4, 27.0:100.4.

2. YBaltisphaeridium sp. S 2389/1, 39.0;95,0. (Nomarski Interference.)

. Limitisporites movcrsensiy (Grebe) Klaus, 8 2267/4, 25.5:110.8.

. Laevigatasporites flexns Segroves, S 2267/4, 25.811 103.

” 19,

"20,

eo. 21.

. Parasavcites gondwanenyty (Balme & Hennelly) Segraves, S 2267/2, 36.8:109 7

- Parasaccites sp. A, 8 2419/1, 4). 2112.4,

» Sulcatisporites sp. cf, S. splendows Leschik, 5 2390/3. 20.0: 109.1.

?Hoffmeisterites sp.. S 2390/5, 39.6: 109.6.

Geminespara lemerua Balme (reworked Devonian example), S 2267/4, 99,6404

Limitispovites sp. of. 1. zecths Leschik, S 2388/3, 32,4:92.8,

PERMIAN SEQUENCE AT WATERLOO BAY 39

AY (

do nor Oeeur an Muviil deposas”. Data from

SAG. Cootatoorina No, ) CArckariney Basin,

Harris & MeGowran 1973) are it keeping with

this conclusion and suggest a threshold salinity

is requiree for their Sppearanee.

Within the Permin sequence al Waterloo

Bay the vsseciation of spmose aeritarchs and

ariaceous Foraminifert ts taketh to midivaie

unequivocally marine conditions, Further-

mote, a dow selinin marine emuronment is in-

ferred from the following:

(1) The presence of Borrvococetis bratutii

within ihe assemblage. This is generally

rumirded as a fresh wuter species (Blackburn

1936; Duthuriv 1944) although Cookson

(7983) has recorded B. brani From Recent

brackish walter environments,

(2) The meagre foraminiferal assenmblige

consisting of only a few specimens (LR) of

upparently only a single species, Hertidiseny

bale’ Ladbrook IAT which is a primitive

form, far which uw low salinity envirenment

seems likely (Harris & McGowran 1971).

(3) The excellent preservation of the miv-

spores, in particular the reworked Devontin

forms. Tsehudy (1969) has shown that such

preservation wauld best be achieved under low

pH, negwive Eh canditions where bicterial

aelivily is minor, Such conditions are

commonly developed on hake bottoms and in

closed basins; Le. not normal murine situations.

Accordingly it is believed that the Permian

sequence pt Waterloa Bay was deposited in a

low salinity onuine or quasimaripe enyiron-

ment.

Evidence of Permian glivial activity within

the Troubridge Basin, particularly on Fleuricu

Pemisula (hig. 1), has been well documented

(see Ludbrook 19699). At Waterloo Bay

vlaucial influence is indicated by erratics und

rare faceted pebbles which occur within the

sequence. Accordingly cold climatic conditions

are inferred. This view is also maintained by

Ludbrook (1967, 19699) and Harris & MeGow-

rin (1971) wha have stated that the aren-

uceous foraminiferal assemblages are also con-

sistent wilh cold water conditions (see above).

Moreover troughs or fiords have been postu-

litect as the sites of deposition of the micro-

faunas (Ludbrook 19694).

The diversity of the microflaral assemblage

at Waterloo Buy suggests, however, that con-

ditions were not fully glacial and that the cli-

Mate Was becoming warmer. In a comparative

study Of microfloral assemblaves (Stave 2)

RO FOSTER

from Antarctica, South Americ and Pakistan,

Kemp (1973, p. 48) concluded it was likely

that the sediments extimined “represent a late

sluge in the ghicial history of the areas

stucicd™.

An active leclome environment covering all

af southern Australia has heen proposed hy

Woplner (1970) and MeGowrar (1973). Both

Workers hive postulated that unittal rifting

between Australia and Antarctica occurred

during this time. Although there is little

olher evidence from the present study. it is

most Itkely that the sediments were deposited

ut graben strayctiies formed by syhgenetic

Yaultinw (see Woptner 1970), The imprediate

cnvironnicat of deposition using this noel is

the same us that proposed hy Ludbrook

(19694). although “Alpine type” glacial

features us proposed by Campana & Wilson

(1955) would not be present.

Syrithesns

From the =o microflaral evidence orl oy

postulated that the period of glaciation was

ending. Svndeposiional movement. in particu-

lar uplift during deglaciation, rejuvenated

erosion and increased sedimentation rates,

Rapid rates of sedimentation are supported by

the presence of unullered biotite, which forms

a significant part of the micaccous clenrent af

cliystones (see Woptner 1970). and the excel-

lent preservation of the reworked Devonian

iniaspores, Such preservation demands rapid

recycling Within a reducing envinpoarent.

There is clear evidence that during this

period a iurine idgression occuited. ft is sie

vested that) inflowing glacial oo mellwaters

appreciably lowered the salinity of the ingress-

ing sea and Consequently restricted faunis to

aveniecous Foraminifera,

This model, consistent with known sedi-

mentologicul and palacontological = dali,

equates the sediments of Waterloa Bay with the

sccond marine shale umt of Wopmer's (1969)

three-part lithological sequence for the Per-

mian of South Australia. The younvest unit.

generally a fresh water deposit, has not been

recorded within the Troubridge Basin.

Conclusions

From the results of a taxonomic study

given. in this. paper, the Waterloo Bay Assem-

hlage is correlated with Evans’ (1969) “Stage”

2 microflora (lower Dalwood Group, Sydney

Basin) and equated with the “Microbaculis-

pora Assemblage” (Nangetty Formation, Perth

PERMIAN SEQUENCE

Basin}, This and the gross quantitutive micro-

faral data indicate a probable Sakmarian

(Early Permian) age.

The stratigraphic seyuenve described is of

local Impertance and includes two Cainozore

discoveries; the dating of the Tertiary lime-

slanes at Late Eocene, and a further record of

planktonic Foraminifera within the Quaternary

acolianitic sequence.

From u consideration of the palynomorphs

and associated arenaceous Foraminilera, a low

salinity environment of deposition was con-

cluded. It is thought to have resulted from

glacial meltwaters lowering the salinity of an

ingressing sea,

Acknowledgements

{am mdehted to the following who have

ailted this study: G. F. Whitten (Deputy

Director of Mines, South Australia) for erani-

AT WATERLOO BAY 41

ing permission to use the Palynological

Laboratory of the Geological Survey of South

Australian, where much of this work was

originally undertaken; Drs. B. McGowran and

K. Jenkins (University of Adelaide) who aug-

gested and supervised the Honours project

from which much of this paper was taken:

Wayne K. Harris (Geological Survey of South

Australia) for encouragement and generous

Provision of laboratory and palynological

library facilities as well as much unpublished

data (particularly Fig, 4); J}. M. Lindsay

{Geological Survey of South Australia) who

provided biostratigraphic information for the

Cainvzoic foraminiferal assemblages; Dr. G.

Playford (Universily of Queensland) for

advice and criticism; Geosurveys of Australia

Pty Ltd. who kindly provided bore hole

sumples from Peesey Swamp Noa. 1 and in

particular A. T. von Sanden who provided

steatigraphic information about the samples:

R. F. Harris and others. for helpful discussicn.

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morphs to. Sedimentation, In Tschudy, R. H.,

& Scott, R. A. (Eds.}, “Aspects of Palyno-

logy”. pp. 79-96. (Wiley: New York.)

Watrernouse, J. B.. (1970)—Correlation of

murine Permian faunas of Gondwana. Prac.

2nd Gondwana Symp. S, Afr., 381-394.

Worrner,, H. (1969),—Deposilional history and

tectonics of South Australian sedimentary

basins, #th FE.C.A.F.E. Symp. Canberra,

E.C.A.F.E. doc. 1, NR/PR4/57.

Woprne_er, H, (1970),—Penmian palaeogeography

and depositional environment of the

Arckaringa Basin, South Australia. Proe. 2nd

Gondwana Syinp. §. Afr., 273-291.

STUDIES ON SEASONAL ANAEMIA IN THE ROTTNEST ISLAND

QUOKKA, SETONIX BRACHYURUS (QUOY & GAIMARD)

(MARSUPIALIA; MACROPODIDAE)

BY §S, BARKER*

Summary

BARKER, S., (1974) .-Studies on Seasonal Anaemia in The Rottnest Island Quokka, Setonix

brachyurus (Quoy & Gaimard) (Marsupialia; Macropodidae). Trans. R. SOC. S. Aust 98(1), 43-48,

28 February, 1974.

A population of the quokka, a small marsupial, lives on Rottnest Island, which lies off the west

coast of Australia. Most of the annual rainfall occurs during the winter and there is a summer

drought. During the summer no free water is available to quokkas living on the West End of

Rottnest I. Water is available at this time to quokkas living in the centre of the island. The

population of quokkas undergoes an annual weight cycle and an associated cycle in haematological

condition. They are at their peak weight and their blood counts are normal at the end of spring. By

the end of summer, there has been a large decrease in body weight and an associated decline in

haematological condition. The factors contributing to the cycle are reviewed. Depressed food intake

during the summer leading to inadequate nutrition is probably the major cause of the observed

cycle.

STUDIES ON SEASONAL ANAEMIA IN THE ROTTNEST ISLAND

QUOKKA, SETONIX RBRACHYURUS (QUOY & GAIMARD)

(MARSUPIALIA; MACROPODIDAE)

by S. Barker*

Summary

Ranken, S., (1974).—Studies an Seasonal Anaemia in The Rotinest Ixland Quokka, Sefonix

brachyurns (Quoy & Gaimard) (Marsupialia; Macrapodidae}. Trans. R. Soe, &. Atisi.

98(1), 43-48, 28 February, 1974,

A population of the quekKa, & small marsupial. lives on Rottnest Island, which lies off

the west. coast of Australia. Most of the annual rainfall occurs during the winter and there

is @ summer drought, During the summer no free water is available io quokkas living on

the West End of Rottnest I. Water is available at this time to quokkas living in the centre

of the island, The population of quokkas undergoes an annual weigh! cycle and an associated

cycle in haematological condition.. They are at their peak weight and their blood counts arc

normal at the end of spring, By the end of summer, there has been w large decrease in body

welght and an associated decline in haematological condition. The factors contributing 1 the

cyclo are reviewed. Depressed food intake during the summer Jeading to inadequate nutcilion

is probably the major cause of the observed cycle.

Introduction

Rottnest Island, lying west of Fremantle,

Western Australia, was named hy de Vlamingh

in 1696 after the small wallaby that was abun-

dant lhere at that time and which he mistook

for a todent. This wallaby, the quokka Setonix

brachyurys. (Quoy & Gaimard}. is still abun-

dant on the island (Hodgkin & Sheard 1959)-

The tolal urea of Rottnest is 1900 ha, of which

200 ha is covered by salt lakes. Fresh-water

seepages occur on the shores of several of

these and ure important as water sources for

the quokkas during the summer,

The island is 9.7 km long and 4.8 km wide

al the maximum width and the long axis Is

orientated roughly east-west. At 6.4 Km Crom

the eastern end, the island is constricted to a

narrow Heck of land some 180 m wide and

further west the island broadens out to a maxi-

mum width of 0.7 km. The part of the tsland

west of the narrow neck is known by the get-

eral name of West End. All of the salt lakes,

secpages and the few fresh-water soaks are

confined to the middle and eastern end of the

island and none are known further west than

near the main lighthouse, situated on the high-

est hill which is in the middle of the island.

Weather conditions on Kottnest T.. are simi-

lar to those on the nearby mainland, except

that annual sainfull (734 mm) is 150 mm less

and maximum and minimum temperatures are

less extreme. The overall pattern is ane of win-

ter rainfall and summer drought. During sum-

met, maximum daily temperatures can be in

excess. of 38"C and temperatures above this

figure have been recorded during November-

March. Mean rainfall during the same period

is 14 mm per month in November und March,

10 mm in December and February, and 6 mm

in January. No free surlace water is available

to West End quokkas in the summer except

after ocessional thunderstorms when surface

pools may form but quickly disappear. The

season usually breaks in April when general

winter rains commence. Maximum monthly

rainfall occurs in June.

When Europeans first settlad tm Western

Australia, the predominant trees an Rottnest

I, {Somerville 1954) were the Rottnest ping,

Callitris preissi Miq., ti-tree, Melaleuca pube-

sceny Schau., and coastal wattle, Acacia ras-

tellifera Benth. Since the estublishmemt of a

prison on the island in 1838, changes occurred

in the vegetation caused by cleuring, fires and

overgtazing by quokkas (Storr 1963}, At the

present time pines have almost disappeared,

wattle now occupies only a small area and ti-

trees accor sporadically. The predominant

* Department of Zoology, Uhe University of Adelaide, Adelaide. S. Anst, 5001.

44 5. BARKER

plaut ussociation which fras increased iit area

since settlement is a heath of Acanthecanns

preissit Lehm,-Sripa variabilis Hughes (Storr

et al $959), The samphires, Arfiiroenemum

arbuscula (R Br) Mog, 4. felocnemoides

Nees, and Aalicermia australity Banks et Sol,,

grow around the salt lakes and soaks, some of

which are fringed hy swordgrass, Galinia rrifida

Labill., and the sedge. Scirpus neduyus Katth.,

both forming a dense cover heavily utilised hy.

guokkis. A flora list has been published by

Storr (1962),

The quokka if one of the small members of

the family Macropodidae. Adult females weigh

from 2.5:3.0 kg and adult males from 3.5-4.5

ke. Its relationships with the rest of the group

have heen discussed by Sharman (1954) and

Ride (1957), Moir ef al, (1954. 1956)

described = ruminaut-like digestion in the

qunkka, which has 4 well developed bactcrial

popvlation in the fore-stomach and pre-gastric

fermentation. Blood glucose and plasma vola-

tile fatty acid concentrations abe intermediate

between (hose of ruminants end rabbits (J.

Barker 1961).

Quokkas occur all over Rottnest 1, bur duv-

ing summer those living in the central part of

the island congregate in the vicinity of Fresh-

water seepages on the edges of che salt takes

and near the fresh-water soaks, They graze the

mat of salt-water couch, Spurebolus vireinious,

(L.) Kunth. so close that it becomes a typical!

‘marsupial lawn’, similar to those seen in Tas-

mania (Ridpath 1964) and other areas of

Australia. They live in high density on the

eastern end of the island. under the houses

used for tourist accommodation, and they are

addicted gatbuge feeders. ‘The smallest popula-

lion probably occurs between the main fight-

house and West End. There seems to be a

fairly constant population (Niven 1970)? ving

wu West End, which shows local feeding move-

mens during summer (Nicholls 1971), They

do fot migrate from West End to fresh-water

sources during the height of summer or indeed

ut any time of (he year (Dunnett 1962)-

Work on the ecology of the quokka, popu-

Jatin) Of Rottnest T commenced with a teg-

ging programme if November 1953. The sum-

mer of $953/54 was het anc dry and hy

March 1954 many yuokkas were emaciated

and same were dying. Research was com-

menced to find out why animals were dying

unl what factors were controlling population

numbers (Waring 1956). The progress made

on these problems is the main subject of this

paper.

Seasonal Ansemia

In 1953 it was found that huemoglobin con-

centrations of quokkas caught in the centre of

the island in simmer were much less thao

those of quokkas kept in the yards af the

Zoology Department, University of Western

Australia, wt the same time of the year {War-

ing 1956). The first possibility considered was

the occurrence of a seasonal deficieney of cop-

per, cobalt or both, It was known at that tinve

that the quoakka had riminant-like digestion

(Moir et ai 1954, 1956), that sheep quickly

dic on Rotinesct from copper und cobalt defici-

ency, und that deficiencics of both copper and

vobalt in ruminants result in anaemia. By

analoy, the same deficiencies might have been

affecting the quokkas, Barker {unpublished)

collected serwm sumriples front animals captured

ul West Eud and at lake Bagdad over an 18

month pertad. The samples were assayed for

Vitamin By (by the Hacmutolozy Depariment,

Royal Perth Hospital) using Bugle as the

fest organism. Mcan serum yilamm Bis ¢on-

centration of unimals caught near Lake Bagdad

was very much greater than that of animals

caught at West End al all times of the year

(means varying between 2.000-4,500 pg/ml as

asuinst a mean of around 1,000 pg/ml). The

West End animals showed 4 slight annual

Aurtuation with the lowest mean serum vilit-

min Bye concentration im the spring and the

hizhest in summer None of these animals had

concentrations low endugh to indicate copalt

deficiency when compared to dhe voncenira-

tions meysured mn animals that had been fed

very low cobalt intakes for several munths

(Barker unpublished),

Blood copper analyses of Lake Bagdad

qguokkas showed a positive correlaiaya with

hacmoglohin coitcentration but this relation-

ship was not found in West End quokkas. 1

was considered that only in the Lake Bugdad

population “was copper deficiency likely to

exert any ellect on blood parameters and then

it was only likely to be one factor associated

‘Niven presented a computer sludy wal suinbers ealenlated From date far the West End quokka

population between 1955-63, based on Holdsworth, W.N. (1964).—Marsupial behaviour with special

referenee ta paputatiom homeostasis in the quokkas on the West Find of Rottnest Island, Ph.D, thesis.

University ot Western Australia (unpublished).

SEASONAL ANAEMIA TS THE QUOKKA 45

with tite develapment of seasonal anaemia

(Burker 1961).

Shield (7959) found that, haematulayical

counts fluctuated with season and wer¢ ¢orrela-

ted with changes in body weight, Adult

quokkas from West End and from around

Lake Bagdad were in peak condition in rhe

spring, Their body weight was maximal and

their blood counts were normil. By the end of

summer there was 4 mean decline of up to

25% in body weigh! and there was a similar

reduction in red cell parameters. here were

differences between quokkas caught in the two

areas in that West Enc animals showed higher

Maxima in spring and lower minima in sutomna

than those trom Luke Bagdad.

The possibility of disease causing the anae-

mis was discounted. as white cell counts were

lower in the summer than in the winter, where-

as tt would be expected thal white cell oum-

bers would increase if disease accurred in the

summer. Dehydration was not thought te be a

contributing. Factor to the decline in condition

of West End animals, as Shickd (1959} had

found that quokkas kept for 6 months without

aceess to drinking water, lost weight but had

ingreased plasma protein concentration. [fow-

ever, it is unlikely that West End quokkas

would experience such severe dehydration.

Storr (194dq) culculated that they had a daily

water intake of jbout 130 ml gained fram

water contained in their plant food. Shield

(1959) found that in West Fnd quokkas,

haematocrit and plasma protein concentration

declined dunng the summer period. In a later

study (Shield 1971) he found that plasma vol-

ume of field animals was unchanged through-

out the year. Clearly, the field animals were

hot cxperiencing the acute dehydration seen in

the yard animals that did not have uccess to

drinking water, However, the possibility that a

fesser or more chronic degree of dehydration

fy o¢cucring im the field cannot be excluded

and this could aggravate the quokkas’ condi-

tion. As a resuli of bis studies, Shicld (1959)

(Main er af. 1959) suggested thal the quokkas

were alfected annually by ‘severe semi-starva-

tion’. which Main (1968, p. 99) interpreted

as protem deficiency:

In a study of the planis eaten by ihe quokka,

Storr (19640) made calculations of the nitro-

gen and water intakes of quokkas from differ-

ent localities om the island a! different times of

the year. The figures he used for nitrogen

requiremenis of male quokkas Were those of

Brown (1964)* from one arhilt male quokka

used in two series of nitrogen balance irials.

Extrapoluting fram this data, Storr (19648)

stated that an adult male quokka requires 0.6

g N/day to remain in positive nitrogen bal-

ance. He calculated mean nitrogen intake al

different localities on the island at different

times of the year and concluded that quokkas

ut Cape Vlamingh had a large surplus of nitro-

gen in winter and a varying deficit in late

summer. There is no doubt that Storr’s use of

the data of Brown (1964) is an oversimplifi-

cabon: for example 3 of the 4 adult male

quokkas used in a feeding trial hy Calaby

(1958) were in negative nitrogen balance,

although their daily nitrogen intake ranged

from 13-16 g@ N/day. The diets used by

Calaby Were net comparable to ¢hat uscd by

Brown (1964).

Barker ef al. (1974) collected blood sam-

ples from one sub-papylation of quokkas living

on West End it spring aad at the end of sum-

mer (197/71), The weight differences

between the snimals im spring and autumn

were marked, yet mean plasma urea concen-

trations were sinular. The ficld plasma urea

concentvalions found by Burker er al, (1974)

were significantly less than plasma trea con-

centrations found in a group of male quokkas

fed on high-protein food for 3 mouths prior

to feeding them a low-protein dict. In this

experiment it was found that quokkas wilh u

low nitrogen intake (= 0.3 g N“/day) and

given walter ed Hh, had plasma urea conven-

tration reduced to 20 mg/100 ml! within four

weeks. Thereafter plasma urea concentrations

of most animals rose, Plasma urea concentra-

tions of quokkas fed the same diet but with o

restricted water intake, fell to 40 mg/ 100 ml

and then remained at this concentration

This pattern has not been found in the Kan-

garoo Island wallaby im a similar type of

experiment (Barker et al, 1970). Wallabies fed

on & low nitrogen diel showed a progressive

fall in plasma urea concentration over a tywo-

month period. Ih a proup fed a similar diet

but with restrigted water intake, plasma urea

voncentrations also fell hut remained higher

than fn the control proup througheut the

experiment. It seems mest probable that in

both the experiments with the quokka and

“Brown, G. D. ( (964). —The nitrogen requiremenis of macropod marsupials, Ph,D. thesis, University

of Western Australia funpablished).

an S BARKER

Ratigarod Island wallaby, the higher plasma

urea concentration in water restricted animals

i8 a Tefiection of a lnwered and inadequate

energy intake. Water restriction below the ad

fib. Intake results in om immediate decline in

appetite and thus ia dry matter intake, The

uctual reduction in dry matter intake appears

to be correlated with the severity of water

restriction comparcd with the ad Jib. intake.

This seems to be constant in individual animals

though it fluctuates widely between individual

animals.

Two isolated short-term studies have also

been carried out on Rottnest I. quokkus, Her-

rick (1961) measured adrenal ascorbic acid

concentration of Retinest I. and experimental

unimals to determine changes tn adrenal fonc-

tion during summer stress, but his Tesults were

inconclusive. Packer (1968) counted eosino-

phil numbers in blood samples taken frum

auokkas on Rottnest I. at different times of

ihe year to determine whether changing popu-

jalion density caused changes in circulating

easinophils. He found no consistent trend that

sugecsied changes at different times of the

year.

Nature of the Summer Stress

So Jur the only evidenve of disease affecting

the quokkas on Rottnest I. has come from the

work of Gibb ev al, (1966) who deseribed the

occurrence of Toxoplasmosis on Rottnest T. but

mmily from animals captured in the vicinity of

the settlement on the eastern end of the island.

Tt is expected that pther infective agents will

eventually be deserthed after a diligent search

has heen made for them, but very little

research effort has been made in this impor-

tant direction,

The key ta summer survival for the quokkas

uo West End is probably their success or other-

wise in Obtaining walter from their food

plants. No permanent source of Iresh-water is

known to occul further west than the main

lighthouse durmg the summer. However, on

the night of March 22nd, 1957, the writer and

Dr E. P, Vodgkia of the Department of

Zoology, observed about 20 quokkus on a nat-

rew beach in Green Island Bay, beneath a low

cliff, The animale were lined up ai the water's

edge aid were upparently drinking sca water.

Trum close observation it was seen that the

animals were digging holes in the sand, near

to the water's edge. before drinking, Water

saiiples were taken from some of these holes

and frum the sea soine 12 inches from where

the quokkas were drinkmg. Analysis of the

samples showcd that the water sampled trom

the hole in the sand was much fresher than

sea-water (Cl 0,519) while that taken from

the sea (Cl 1.61% ) was slightly less salty than

normal sea water (Cl 1.99%}, Casual observa-

tion withiul collecting water samples would

have led ys to the conclusion that the quakkas

were drinking sea Water. As Bentley (1955)

found that the quokka can maintain walter

balance under laboratory conditions drinking

2.5% NaCl {but not sea water) it seems

reasonable to assutie that animals drinking

scepage water were able In maintain a positive

water halance-

Although water is cssenttal for Lhe main-

tenance of fluid space, excretion and tempera-

ture regulation, one of the first manifestations

of water shortage is depression of appetite. To

an animal that may have to forage for suitabic

food over tong distances and sutvive the

stress period on a marginal dic, Irom an

energy paint of view, this could lead to a

slowly worsening starvation state, The animal

would gradually lose weight, become weak,

and unless there was relief from a change in

the seusem, it could eventually succumb. Storr

{1964a) indicated that although quokkas

which teed on Carpobratuy al Cape Viamingh

may get sufficient water from this plant to

imect their neets, their nitrogen intake would

certainly be reduced below a reasonable intake

for maintenance purposes and such animals

could fil into the scheme outlined above.

Water is also am essential requirement for

thate unimals living close to freshwater

soulves, particularly ducing summer and this

fact has heen expluited for the capture of large

numbers of quokkas (Dunnet 1956). Access

to water silone, however, is not sullicient for

the maintenance of constant blood piirameters

Both Shield (1959) «and Barker (1961)

showed that in animals with access tn drinking

water haemoglobin concentrations fell during

the summer though not as dramutically as in

animals captured on West End.

Despite a great deal of work and speculation

on this problem,. there 1s still no clear-cut

answer to the question of the nature of the

stress experienced by quokkas during the sum-

mer and early winter. It is probable that some

animals surviving summer stress, but debjilita-

ted by it, are killed off when the scason breaks

and they are faced with cold and wet condi-

tions. Barker ef al, (1974) found that 8 uy of

11 yuokkas that had survived for 8 weeks on

a low nitrogen intake, died in 10 days when

SEASONAL ANAEMIA IN THE QUOKKA 47

might and early morning temperatures fell uver

a shert period.

There is a strong possibility that. lhe popula-

tion al West End faves & more severe suress

than those in the central parts of the istanil.

At West End, quokkas almost certainly face

a less than adequate water intake, excep! for

those feeding on Curpebrotus at Cape

Viamingh (Sterr 1¥64a), 9s well as nutritional

stress. Quokkas living in the centre of the

island Face a nutritional stress only, water being

available. A water shortage at West End would

result in quokkas having a decreased dry mat-

ter Intake causing a lowered nutritional status

leading to anaemia, WFP nitrogen intake of

quokkis m the Lakes area becomes inadequate

in summer, dry mytter intake would be

depressed also leading (o anaemia. The nature

of the anuemia developed at each area would

be similar despite a different origin (Barker

ef al. 1974).

Inadequate water intake does not necessarily

lead to haemo-concentration (Barker ef al.

1974). Shield'’s (1959) conclusion that water

intake is. not limited on West Bnd in summer

was based on the results of his experiment

Where no-waler whatever was provided for the

experimental animals. This situation never

occurs on West End as although muisture con-

tent of food plunts is reduced during summer

(Ston 19648), the reduction jn water intake

is nat likely to be myzh ereater than half of

the ad Jif, requirement. Shield {1971} showed

that a decrease in hlood volume does occur in

West End animals duriag the autumn relative

to blood volumes of Wost End animals meas-

aired in the spring. However, (he difference was

due to & reduction in red cell mass, not in

plasma volome. a finding not incompatible

wih the thesis of a restricted water intake

exerting a pulritional effect through loss of

appetite.

Although the figures for nitrogen requise-

ment of the quokka piven by Storr (19642)

are too limited to be conclusive, it seems from

his data that nitrogen intake al West End

could be less than the maintenance require-

ment. However, the possibility that nitrogen

shortage alone causes the debility seeins remote

if « complex situation, where nitrogen is likely

to be only one of sevaral compenents of the

diet which are seasonally deficient,

Fitture of the Rottnest Quokka

Despite the obviously deteriorating ebyiren-

ment on Rottnest 1, caused mainly hy human

activities but also affected hy natural eroston,

the quokka population is. surviving. Some of

the differences between the Rottnest J. envir-

onmentinel that of one area where the quokka

sull occurs on the adjacent mainland, have

been outlined by Storr (1964b). In ane way,

Rottnest is totally unlike the mainland situation

in Chat no predators are present. If they were.

the population would be reduced as those

animals weakened by scasonal influences would

fall casy prey te a predator,

The quekka has a considerable and unique

value as a Natural resource and ii Is to be

hoped that it has u guaranteed Future on Ratt-

nest I. ‘Ihe value of the island #8 4 draining

ground for scientists has been stresacd hy

Main (1959, 1967) and this is largely because

of the occurrence there of the quokka. How-

ever. the greatest value of the giiokka Ties jn

its asset as a tourist attraction. 11 is to be hoped

that the Western Australian Governmeni

Tourist Bureau, which controls the tsland, does

not underrate this asset and takes positive

steps towards ensuring the permanent survival

of the quokka on Rottnest I.

Acknowledgements

1 am indebted to Professor P, Bentley, Dr.

I. G. Jarrett and Mr, D, Kabay for criticisny of

the manuscript. The University of Adelaide

provided funds which cnabled me ta wark in

the Department uf Zoology, The University of

Western Australia where this paper was wril-

ten during sabbatical leave, T am grateful to

Professor H, Waring for accommodation in

his Department.

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Moir, R, J... Somers. M., SHARMaN, G., & WARING,

H, (1954).—Ruminant-like digestion in a

marsupial. Nature 173, 269.

Meum, R. J. Sommrs, M.. & Wanine, H. (1956).—-

Studics on murcsupial nutrition, 1. Ruminant-

like digestion in a herbivorous marsupial

Setonin brachyurus (Quoy & Gaimard). Aust

4 bial, Ser. 9, 293-304-

NicHoiits, D. G. (1971)—Daily and seasonal

movements of the quokks, Setonix brachyu-

rus (Marsupialia}), on Rottnest Island, net,

J, Zool, 19, 215-226.

Niven, B. §. (1970),—Mathematics of popula-

tions of the quokka Setonix Arachyurus (Mar-

supialia), [. A simple deterministic model. for

quokka populations. Aust, J, Zonl, 18, 209-

214.

Packer, W. C. (1968).—Easinophils and papu-

lation density in the marsupial) Seleanix, J.

Marmm. 49, 124-126.

Ripe, W. D. L. (1957),—Profemnadon parma

(Waterhouse) and the classification of relaicd

Wallabies (Pratemnadon, Thytogale and Ser-

onix). Proe, Zool, Soc. Lond. 128, 327-346,

Rippatu, M. G, (1964),—The ‘Tasmanian native

hen. slat. Mat. Tivt, 14, 346-350.

SHARMAN, G, B (1954),.—The relationships of

the Quokka (Selonix brachyurusy). Wo Aust.

Nat. 4, 159-168,

Sutecp, J. W. (1959).—Rotinest Field Studies

concerned with the Quakka. J. R. Soc. W,

Aust. 42, 76-78,

Snetp, J. W. (197L)-—A seasonal change in

hlood cell volume of the Rottnest Island

Quokka, Setonix brachyurus. Po Zool. Land.

165, 343-354.

SOMERVILLE, W, (1954),—"Rottnest Island". 2nd

ed. {Rotinest Island Board of Control: W.

Ausl,),

Storr, G. M. (1962).—Annotated flara of Rott-

nest Island. Western Australia. W. Aust. Nat.

8, 109-124.

Store, G. M, (1963).—Some factors inducing

change in the vegetation of Rottnest Island.

Ww. Aust. Nat. 9, 15-22.

Stora, G, M, (19648)—Studies on marsupial

nutrition IV, Diet of the quokka, Setanix

Arachynrey (Quoy & Gajimard), on Rottnest

Island, Western Australia, Aust. J biol. Sci.

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Storr, G. M, (1964b)—The environment of the

quokka (Setonix brachyurns) in. the Darling

Range, Western Australia. J. RK. Soc. HW’. Aust.

47, 1-2.

Siorn. G, M., Green, J. W., & Cuurcuini, D. M,

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VOL. 98, PART 2 31 MAY, 1974

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Houston, T. F. Revision of the Amphibolurus decresii Comes (Lacertilia:

Agamidae) of South Australia - = = - 49

Watts, C. H. S. and Aslin, Heather J. Notes on the Small Mammals of North-

Eastern South Australia and South-Western Queensland - - 61

Tyler, M. J. and Parker, F. New Species of Hylid and a -Leptedactyhd Bor from

Southern New Guinea - - - - 71

Jamieson, B. G. M. Earthworms (Oligochaeta: Megascolecidae) from South

Australia - - - - - - - - - - 79

PUBLISHED AND SOLD AT THE SOCIETY'S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

REVISION OF THE AMPHIBOLURUS DECRESIT COMPLEX

(LACERTILIA: AGAMIDAE) OF SOUTH AUSTRALIA

BY T. F. HOUSTON*

Summary

HOUSTON, T. F. (1974).-Revision of the Amphibolurus decresii complex (Lacertilia: Agamidae)

of South Australia. Trans. R. Soc. S. Aust. 98 (2), 49-60, 31 May, 1974.

The taxonomy of the rock-dwelling dragon-lizards of the Amphibolurus decresii complex is revised.

Two previously established taxa, A. decresii (Duméril & Bibron) and A. fionni Procter,

are tentatively maintained as species while a third species, A. vadnappa, is described as new.

Each species is composed of two to several races distinguishable mainly on the basis of male

coloration. Strict preference (except perhaps in juveniles) for rocky cover and past changes in the

distribution of rock outcrops are presumed to have been major factors in evolution of the complex.

REVISION OF THE AMPHIBOLURUS DECRESII COMPLEX

(LACERTILIA: AGAMIDAE) OF SOUTH AUSTRALIA

by T, F. Houston*

Sommary

Houston, T. F,

(1974).--Revision of the Amphiboluras decresit complex (Lacertilif:

Agamidue) of South Australia. Trans, R. Soe, 8. Aust, 98% (2), 49-60, 31 May, 1974.

‘The taxonomy of the rock-dweljing dragon-lizacds of the Anrphibolurys decrevi Complex

ix revised. Two previously established tuxa, 4. deeresii (Daméri) & Bibron) and A. iow

Procter, are tentatively maintained as species while a third species, 4, vadntappa, ts deseribed

ws new. Each species is composed of two to several races distinguishable mainly on the basis

of male coloration, Strict preference Cexcepi perhaps in juveniles) for rocky cover and past

changes in the distribution of rock outcraps are presumed to have been mujor factors in

evolution of the complex,

Introduction

The species-complex dealt with here includes

the Tawny Dragon, Amphibolurus decresit, the

Peninsula Dragon, A- fiomni, and several forms

hitherta undescribed. The lizards inhabit an

area of South Australia bounded by Ceduna

in the west, Marree in the north and Kangaroo

J, in the south, and which extends east to

Modtwingee in western New South Wales (Fig.

1),

Much confusion has arisen around the com-

plex and the need for a taxonomic revision has

long been felt, A wide array of colour patterns

occurs amongst adult males from different areas

with little or no corresponding morphological

diversity and without comparable colour varia-

ion in Females and juvenile males. Thus, while

the geographica) origin of an adult male may

he determined from its colour pattern, this is

seldom possible with females or juvenile males,

Unfertunately, the name 4. fionn was based

only on the female sex and no accurate indica-

tion of the type locality was given, The descrip-

tion fitted females fram most areas and the

applicability of the name to a particular male

colour form was left in doubt. The status and

nemenclature of the different male colour

forms were variously interpreted with resulting

confusion in collections.

The present study included examination of

over 300 specimens in the collection of the

South Australian Museum and field ohserva-

lions in many parts of South Australia, It has

become clear, however, that a full understand-

ing of the complex cannot be obtained without

detailed behavioural and ecological studies,

This paper is intended to clarify nomenclature

as fur as presently possible, to facilitate such

studies now being undertaken elsewhere.

All specimens listed in this paper are in the

South Australian Museum and, unless other-

wise indicated, all Socaiitites mentioned are in

South Australia.

Diagnosis of A. decresit complex

Lizards of moderately to strongly depressed

form, up to 25 cm long (snout-vent Iength <=

96 mm); nostril below a sharp canthus rostra-

lis; a weak nuchal crest but no vertebral crest

(at most, a line of perfectly aligned Keels or a

raised fold of skin); dorsal body scales mostly

homogeneous, smooth to obtusely keeled and

subtubercular; skin around tympani, nape and

sides of neck with few to inany spines, occur-

ring singly or clustered on folds of skin; ven-

tral scales smooth; 32-50 femoral and preanal

pores, closely arranged along a more or less

straight line extending full length of thighs hut

interrupted medially: each pore situated

between several scales; lower jaw with dark

imegular reticulations or Jongitudinal lines

{often obscured by bright colour washes in

males); chest of subadult and adult males with

a grey to black patch tapering posteriorly,

* South Australian Museum, North Terrace, Adelaide, & Aust. 5000,

A FIONN!

A DECRESII

A. VADNAPPA

DECRESII and VADNAPPA

100 km

134°

*, F. HOUSTON

Fig. 1. Distribution of Amphibolurus decresii, complex in S. Aust, Broken lines enclose the ranges of

individual races. The numbers are referred to in the text.

sometimes closely approaching vent; males

(except early juveniles) usually with bright

yellow, orange, red, pink or blue patches or

washes; females and early juvenile males

usually dull grey, brown or reddish brown

with black stippling and mottling; tail length

1.4-2.3 times snout-vent length; hind limb

0.7-1.0 times snout-vent length.

Examination of all available material sug-

gests the existence of three major taxa (each

composed of two to several minor taxa) which

I am treating as species, These taxa are dis-

tinguishable mainly on colour differences but

there are also some minor structural features

separating them. The name A. decresii

(Duméril & Bibron) applies to one taxon (in-

habiting areas 6-8, Fig, 1) and the nume A.

fionni Procter to another (inhabiting areas 1—

4, Fig. 1, and Neptune and Wedge Is.). In

view of the very close similarity of these two

taxa, they may not be reproductively isolated,

but until this is clearly demonstrated nomen-

clatorial changes are unwarranted, The third

major taxon (inhabiting areas 5 and 6, Fig. 1)

is the most distinctive of the three and is

partially sympatric with A. decresii. In the

REVISION OF THE AMPHIBOLURUS DECRESH COMPLEX .

absence of known intermediates, it is accorded

species stutus and named here as 4, vadnuappu.

it is mot ® simple matter to clearly define

the three forms because of intraspecific variu-

won, bur the following key should facilitate

recognition of them,

Key tu species of the A, decresii complex

1, Dorsal head scales between und in front of

eyes usually coarsely wrinkled (Fiz, 2), ot

simply keeled; mid-dorgul tow of scales with

longitudinally aligned heels extending at Jcast

partway along hack (more prominent in males

which ure uble to raise a fold of skin along

verlehral line}, adult males with orange oF

reddish spots on sides of body tending to

coalesce to form vertical burs and with a

broad =immaculite vertebral sizipe frour

nape to hase of tail (Figs. 12, 13); mottling

on sides of females often suggesttve of

barring a PM A. yaanappa

|. Dorsal hend scales between and in front of

eyes longitudinally keeled (Fig. 3), sometimes

oblusely so or virtually smooth but (Neptuoe

[, specimens. ¢xcepted) never coarsely

wrkled; no mid-dorsal row of scales with

lpngiludinally aligned keels alomz back {at

most 8 short incomplete row in some A.

decresit): adult males without orange or red-

dish spots on sides of body coalescing inte

vertical burs or, if so, then maculations exfend-

ing across vertebral region (Fig. 11); mottling

on sides of female variable - ’

2. Sides of body with a few to many scattered

tubercles waich are usually pale and can-

trast with ground colour; bady colour pat-

tern of adult male consisting essentially of

a blackish jateral stnipe each side, margined

above and below hy paler iines or rows of

spots; lower jaw of adult male usually

bright yellow, orange, or blue 4. decresié

Sides af borcly without scattered tubercles;

hody colanr pattern of udult male ¢on-

sisting essentially of pale spots or blatches

oflen aligned transversely, sometimes Jaree

nnd coalesting into bars, sometimes

reduced and limited mainly to dorsolateral

folds; lower jaw of adult male usually

with bright yellow wash over greyish

reticulstions but never with right blue

wash 3 AL fianni

Amphibolurus decresii (Dumnéril & Bibron)

FIGS. 1, 4, 14-16

Gramaimophora decrysli Duinérit & Bibron,

BH37) 472-4; 1854, pl. 4), Gigs. 1. [a-c.

Avoma ecreviensis Fitzinger, 1843; 83 (new

Tame for G deeresi? Th & BY).

Crenwpharns deeresii (D. & B,).

1B43- (8, $3,

Ara phtharittis deerent) (D. & B.A, Peters, 1864;

Filazinger.

Typess Tle de Decres (= Kanparoo lt... §,

Aust), collected by Peron and Lesueur,

Dumeéril & Bibron uppurently had several

Specimens of both sexes but did not designale

one as [he type. They figured a male. Goibé

Fig. 2, Phpee scales from tap of snout of Aenphi-

balwrus vadrappa,

Fig, 3, Same from A_ franni.

(1934) recerds the presence of two syatypes

(no. 6345) in the Muséunj National d'Histoire

Natorelle, Paris.

Duméril & Bibrow’s (1854) coloured figure

of an adult male A. decresil clearly shows a

black fateral stripe margined above and below

with pale spots and their (1837) description

mentions small tubercles sprinkled over the

flanks. [ have no hesitation, then, in applying

the name A, decrysii to the populations in-

habiting areas 6-8 (Fig, 1) whieh are dis-

tinguished by these features.

Sourneen, (typicar) Race (Area 8, Fig. 1}

This tace appears to he confined to the

western end of Kangaroo 1. the western

scarps and gorges of ihe southera M1, Lofty

Ranges and the southern margin of Fleurieu

Peninsula. lr is comparatively \niform

throughout this range.

Adult pale putiern:; Head light browns lower

jaw and tips diffusely height blue; throat and

sometimes shouluees bright yellow; black patch

in fold of skin each side of neck usually

separuted by pale brown from blackish lateral

stripes on body.

Female pattern: Ground colour jisually dull

brown of grey-hrown; |ateral body stripes

often developed as in males but black speckting

and mottling ¥ariable.

52 T. FE HOUSTON

Norimnun Racks) (Ateas 6 and 7, Fig. 1)

Males from areas 6 and 7 show far nore

variation in coluur patiern than those of the

southern race. However, | have secn too few

specimens {particularly live males in full

coloration) ta know whether the -yariation

is regionally dependent or individual only, The

bright colour markings and washes about the

head and neck closely resemble thase of some

A. fienni males.

Adult mate pattern: Head usually grey or dark

dorsally: lower jaw teticuluted with grey and

sufused with hright yellow or with a large

orange patch cenirally but never with a bright

blue wash; throat yellow or orange; markings

about ears, neck, pape and sometimes eyelids

ofange.

Female patrerae

smuthern females,

Specmiens Hxaminwo: AREA 6: Arkaracla HS,

R1O916; East Painter Gorge, R1N940: Echo Camp,

Arkarovla Creek, RIV9L7) Mern Merna, R26605

west of Mt Painter Camp, RY0915; Mr Serle.

R5G02, RS59I4: Nooldonnooldogna Waterhale,

R10952; Nomh Tosk, Gammon Range, R3942;

Paraluna Springs, RIG9SK. RLOGSI, RiGS3; Sk.

Mary Peak, R6004; Wilpena Gorge, R3806; LY

kin W oof Wirrenipa. R3753; Yudnamutana Creek,

k3492. RB7E0, RIBW-Z AREA 7; Burrs,

R12492; Clare. R2337; Maotwingee, N.S.W.,

RS1l9d. ML Reéemarkuble. R3306. BG6I79, R953,

near Olary, R12909-10: Pr, Germein Gorse,

R12792; Verawie, R2496; 13 km Sk of Wurciwie

Very similar to that of

via Mawker, R2576; Wilmington, R3724;

Wirrubara, R88621. AREA &: Basket Range,

R2834; Tncounter Bay. Rl686; Fifth Creek,

R435; Glen Osmond, R9379-85; Kanearoo Is,

(RII89; south side, RYO; Harveys Return,

R11260: Ravine de Casours, R3283; West Bay,

Tlinders Chase. R9341); Mentacute, RS802; Nor-

manville, R2881; Onkapurinza Gurge. RY8S4; 32

km N of Peterborough, R11345-7; Sandy Creek

(fh of Gawler), R12075; Second Vallev, R25t5;

neor Tea Tree Golly, RLI358-9: Waterfall Gully,

RI46L, R2037. R2895

Amphibolurus fionni Procter, 1923: 1075, figs.

4a-c.

FIGS, 1, 3, 5-11, 14-16

Holotvpe: 2. coast of the mainland of 8.

Aust., F. Wood-Jones, in B.M.N.H., Lonrlan.

The Jate Dr. M. Smyth, Department of

Zoology, University of Adelaide, who saw the

type, informed me that the accompanying data

record it from Pt, Lincoln, S. Aust.

it is unfortunate that the description of this

species was based on a fFetnale only, for, as

mentioned above, females may be virtually im-

possible to identify with any particular race on

the basis of appearance. Pracies's descriplion

and figure. however, aid a photograph of the

type (Fig. 10) agree closely with specimens

from Eyre Peninsuls,

Severyl distinctive races of this species are

described helow. Since adult males of all races

usually have a dark prey reticulum and yellow

wash on the lower jaw and throat, it is nol

mentiongd among the diagnostic fewtures of

each race,

Nortacen Race (Area t, Fig. 1)

Area 1 corresponds upproximately to what

was ance a large tubleland (Arcoony Table-

land) and now consixts of the low rolling

Andamooka Ranges and series of fsolated

mesas and tenthills. The lizards inkubit the

rocky scarps and stony creek beds.

Adult nutle petterns Dorsal ground yolbur

hrawn gtading to blackish brown on neck,

shoulders and flanks; irregular, often very

dense. pale spotting or blotching an nape, neck,

shoulders and Nanks sometimes coalescing to

farm vertical burs on sides of body (Fig. 11)5

ut least some, and often most, of spots an

flanks orange or reddish, the remainder

white.

Female pattern: Dorsal ground colour brews;

dark mottling on sides of bouy freqnently tens

ing to form) alternating light and durk bars.

This race is very similar in cololation te

A, vadnappe, although it does mor exhibit ihe

distinctly bluish tints found on the body and

limhs of males of that species, nor docs it

huve predeminanity coarsely writikled scales

un top of the snout nor a vertebral keel linc.

Some specimens from the southernmost

lozulity nt Area 1 (Ure Bluil) differ very little

from those of the central race helow,

Crn7eaL Rack (Area 2. Fig. 1)

Area 2 inchides the suuthemmost remfants

of the Arcoona Tableland, the Gawler, Middle

back and Blue Runges and several smaller

ranges aud Isolated hills.

Adulte male putivrn: Dorsal surtage largely

blackish except for brownish head ans grey

limbs and wil; distinet white spots scalleted

over back and flanks cenlinuing [in orange

spols and blotches on shoulders, neck and

nape (Fig, 5); evelids often diffusely orange.

Female pattern: Highly variable; dorsal growing

colour in Gawler Runges specimens reduish-

brown to brick red but brown to grevish in

ther areas; dorsal surface stippled and mottled

with black to varying degrees and often pale

spotted or ocellate in large apecimens.

SOUTHERN Race (Area 4, Fig, 1)

Area 4 cuincides with the south-eustern part

REVISION OF THE AMPHIBOLURUS DECRESIL COMPLEX

Amphibalurus decresii. Dorsal view of adult male from Montacute (Area 8),

« Amphibolurus fionni. Adults in dorsal view. Fig. 5.—Male from Lincoln Gap Stn (Area

2). Fig. 6—Female from South Neptune I. Fig. 7.—Male from Lincoln National Park

(Area 4). Fig. 8.—Female from Marble Range (Area 4), Fig. 9.—Male from same.

‘an

‘ad

Sa T. F HOUSTON

ot a large limestone (caleareous seofianite)

expanse, The limestone is exposed on muny

rises and has weathered to form numerous

rocks and slabs beneath which the dragons

find shelter. A number of granitic and gneiss

intrusions also occur i the area forming pro-

minent hilly with bare rocky outcrops which

gre alsa inhabited.

Adult male pattern: Dorsal ground colour pale

grey with only a little blackish colour on sides

of neck and below dorso-lateral folds an-

teriorly: pile spotting confined in most speci-

mens to folds of skin about neck und anterior

purts of body. especially along dorsolateral

folds (Pig. 9), occasionally occurring over

buck generally but ooly weakly,

Female patter: Wighly vartible: ground colour

wey to hrown: juveniles often finely speckled

hut larger specimens usually have dork

mottling: forming course regular patterns.

sometimes with pale spotting A particularly

hold pattern oceurs amongst femates from the

Marble Range (Pig. 8).

This race has been the husis of several

feports of 4, decresti occurring on Eyae Penin-

sulla, because of the similur colour paliern in

miles of the two forms, However, the absence

of scattered single tubercles on the Manks of

Fyre Peninsula specimens will distinguish them

from a4, decresti,

Since thiy race is the Quly ane known lo

occur in the near yicinily of Port Lincoln, it

may be that to which the holotype belongs,”

Wrsv Coasr Porutations (Area 3, Pig. 1)

Atea 2 includes the northern seetien of the

limestone expanse mentioned above. the Isles

ol St. Francis and the Investigator Group

(Flinders and Pearson 1s.). Pew male speci-

mens are available from this wea so that a

clear pictule of their variation is not yet avail-

abie.

Males from Area 3 differ from those of

Area 4 in their generally larger size and some-

what bolder colour pattern: the blackish neck

patches and Jateral body bands are more in-

tense, 4 pale line or series of spots defines the

blagk neck purehes. and enlarged pale spots

margin the fateral stripes above and below

(Fig. 7). They ure even more like males ot

4. devreyii than are mules of the southern race

Females tend to have patterning similar to

mules but in shades of brown rather than grey.

Without further collecting in West Coast

locahtes one cannot be sure that their A. fiowni

populations do nol intergrade with those of

Area 4.

Nerruny anh Weoae fs. Races

The populations of these lands differ from

those of Arca 4 in colour pattern and then

generally larger adult size,

Adult male patrerns Dorsal ground catour

brown tending to black on neck. shoulders anid

flanks. scattered distimet white spols om nape,

neck. back and base of tuil fending to align in

transverse rows; blackish colorytion intensi-

fied around many pate spoils on back. almost

forming ocelli, Since only preserved specimens

were examined, the presence of bright colour

washes. (other than yellow on the throut) wits

not observed.

Femule pattern: Very similar to male patterns

although generally paler with even more

istinee oeelli and much bhick stippling (Fig.

OH),

Nepuine Is, specimens have conspicuously

rougher and aere mucronate seafes on the

huse of the tail and hind jegs than specimens

frony Wedge tL and olher yreas, They are

also nusual in that the scales an top of the

snout lend to be wrinkled (as in Vig, 2. bur

not sa coarsely). The dorsal snout seales ol

Wedpe bE. specimens are mamly smooth.

While the various rices outlined above show

marked diflerences from one another in male

coloration Viewed overall, there is. cansiter>

able variation within each race and conver-

gence of feajures may be found in specimens

from different races. In view of this, 1 have

preferred ot to erect subspecies of A. frenny.

Sepcimens BXaMINeb: AREA 1; 3 ki SW oot

Bedu Hill, R3877; Bowmans Creck, Bosworth Sin,

RaK33: north-west tip of Carrapateena Arm ol

Lake Torrens, RIG319: Encolo © reek, RIAGO4

R1Z485: eastera Side of Lake Hart, RS065-7

south end of Lake Torrens, R3832; 24 hm S of

Pimba, R6IR9; Uro Bluff RI2832. RII835-6,

R12904: Woodforde Creek, R2795, R279¥. AREA

9: Blue Runge. ROI RLOI73; Carappee Hill.

R933, 212927: Corunnn Hill, R445, R127,

Kondoolka Stn, BRLI7S53: Liacoln Gap Sin,

R}2466-70; Middieback Range. S of Tron Raton,

Ri2079. R1I3055: Ml, Nott, S of Thurlen HS,

6229-30) Payney Stn, R&KU4: South Tent Hill.

24 km WNW of Pi, Augusta, R13054: Tandale

Rock Holes, R12592; ‘Thurlga Sin, R5804, AREA

4: 45 km S of Baird Bay. R9241-2: Flinders L.,

Ri443: Mi Wedge, R57392, RSR3IO. RY243: Pear-

‘ Another rage wis found recently on granite onterops immediately north of Pt, Lincoln by Mr. J

Gibbons. Dept, of Zoology, University of Adelaide, This race, adult males of whieh are siiperficinlly

lke those of the Neptune I, race in coloration, may equally well be ihe typical One.

REVISION OF THE AMPMMBOLURUY DECRESH COMPLEX ab

son 1s. (RINI39, RIOKAES) northern island,

R1O208); St, Francis [. REY6. R3009, RIZSTA:

Streaky Bay, R392, ARPA 4: castern cage of

Bascombes Well Notional Park. R12615; Blesing

Reserye, R9227-40: near Fishery Bay, R2551;

Hincks National Park, RLOIO0O; Hundred of

Nivholls, RLOLOL, R1O1N3-5, RIOLOT-10, RIOVIS.

RIOII6, RIONI9, RIOT78; 19 km NW of Kurkoo.

R947; Lineoln Nalional Park, R12094-4:

southern end of same, RI2926, RiWOSH) Marble

Range. RI29IO; Mikhira JIS, RS7S2-3, 19 kim from

Sheringa, R3626: Sleaford Mere. R&IO2> 4 key W

of same, RIM998. NEPTUNE Is. R230,

RS722-3: south island, R535). Reddo, RIO&79-42-

north ishind, RI2899, WEDGE T: R5340,

RIN636-7, RULSTA

Amphiboluris yadnappa, sp, nov,

FIGS, f, 2, 12, 1a, 1416

Helawpe ¢ {RId16B). Aroona Waters

(138° 21K, 30°35'S). Flinders Ranges. 8,

Aush, 3.1959, PL F. Lawson.

This species inhabits Areas 5 und 6 (Fig,

1), the type locality being in the latter. Prox-

imity of the range of this species to that of the

northern race ot 4. fionni and the remarkably

similar coloration of adult males of hath

forms might sugeest thal they are merely races

Of the one species. However, ihe two may be

distinguished on the features outlined in’ the

key, Adult miles of 4. padnappe also tend to

exhibit a bright bluish sullusion of the chin,

Nanks, uid limbs which iy not known in

horthem A. fount. Some ditferences in body

Proportions also occur (see below),

This attractive species was well known to

Aborigines of the Flinders Ranges {rom whose

fanguage the specific tame has been taken,

the Aborigioes were impressed by the presence

of red bars on the males alone and likened

males to boys uboul ta be initkted who are

painted with red stripes on the back. The

females they likened (o girls who are never so

adorned. ‘Thev call the trzard Tivadnappa’ (‘iti

lizard, ‘yudnappa’ — boy puintec for initia-

tion ceremony). (R. W. Ellis, personal com.

munication ).

The specific name is dsed as a noun and is

not Hable to termination changes.

FRINDERS Rances (Tyriea.) RACK (Atea 6,

Vig, 1)

Head wind body only moderately depressed

(less than the other two species}; neck in

adult males at Jeast as wide as head so that

litier appear to sit direetly on shoulders,

Meusnremenrs of holoivpe: Total length, 252

mim) snout-veot length, 79 ron Gail length, 173

mo hind Gib length. 70 mm: head width, 22

mini, snout-gular fold length, 29 mm; tetal

femoral and preanal pores. +3.

Scalations Scales on top of snout coarsely

wrinkled (Big. 2), seldom almost smooth.

never simply keeled as in Pig, 3; fokis of skin

above and behind ears and on sides of neck

With clusters of small spines (leebly developed

in juveniles and females); scales of fimks very

small, subtubercular and homogeneous. gradiag

into slightly larger. Matter dorsal scales which

ave very feebly keeled, Jlanks without scattered

‘ingle tubercles: a row of perfectly aligned,

longitudinally keeled scales extending from

duehal crest about three quarters of length of

back (less well-developed in females); this

keel line Frequently wecentuated by being raised

on fold of skin.

Adult male coloration: Wead pale brown dor-

sully; broad mid-dorsal stripe from nape to

base of tail und upper parts of limihs und tail

light grey or blue-grey: sides of neck and body

blackish with orange or red spets and blotches

usually partly coulesecd forming irregular ver-

fieal bars (Fig. 12): chest with linge diffuse

black patch anterior to Which skin is bright

yellow, the yellow extending onto throat and

shoulders and occasionally 4s spots along

Nunks;: chin and 34 longitudinal lines on exch

side of lower jaw blue or blueevrey; limbs and

datk ground colour of flanks slightly to

strongly suflused with blac (the yellow, orange,

red und. to a lesser extent, blue colorations

pradually [nde away in spirit).

Female coleration: Dull brown above with

course dark mottling on sides of neck and

body forming uw patlern of alternating, irregu-

lar, light and dark bars; dorsal surface with

scattered blackish spots; lower jaw amd throat

with longitudinal dark grey lines (more

numerous and prominent in juveniles).

WILLOURAN Races. Race (Area 5, Fig. 1)

The Willouramn Ranges, lying west of the

Lyndhurst-Marree road. represent a north-

western spur of the Flinders Ranges system

but ure isolated by wide tracts of sand and

soil plain,

Threesmales from this aren differed from the

typical form io their less robust build ane

narrower necks. The pale spots on their bodies

were smaller and while tending to be aligned

transversely, dict not coalesce tm the same

degree (Fig, 13),

SPULCIMUNS EXAMINED: Paratypes —Anpepeni, 3)

km F of, R3423; Arkaroola, RIOOTR 23, R116),

RL1373; Aroony Waters. RA416 A and ©, RABI 1:

Beltana, R3OOI: Boulder Bore R1OU%4-5: Com-

56 T. F. HOUSTON

REVISION OF THE AMPHIBOLURUS DECRESI? COMPLEX S7

inoore, 9,7 ky NE of, R2819; East Painter

Gorge, last & km of, R10965-7; Echo Camp,

Arkaroola Sin, R10946; Ilinawortina Pound,

R5950; Mi Aroona, R3314A, BR aml D; Mt

Fitton. Moolawatany Sm, R81!4; Narring Stn,

Ri0402-4; Oruparinna National Park, B12749,

RI3053; Parachilna Gorge, R4321; Terrapinng

Springs. R12432, Waukawoadna Gap, 96 km N

of Blinman, R12837; Vudnamutana Gorge, R3492,

R13123; Wilpona Pound, R1O638, Allotype— Mt,

Armona, R&31dC.

Morpho- metrics

Maxinuiun size

The maximum size attained hy adults was

found io vary somewhat between races as

shown in the following table,

Meaximnitte sreteat-veat

lererh in mim

Species or Race {df and 2)

a. deeresté

(Northern) - : 82 73

(Southern) . . - 75 75

Ay fioniti

(Northern) pnt 94 32

(Central) e -_ 78 72

{West Gaast) i S&S 79

(Southern) 77 76

(Neptune Js.) 96 87

These figures suggest 4 north-south trend of

decreasing body size apart from the Nepuine

Is, race Which attains the greatest body size of

ull.

Relative length of hind Kmbs end tail

In this comparison only dala From adule and

subadult specimens were incorporated, since

the relative lengths of appendages deeiease

slightly with increasing body size (i.e, with

age), The lengths of the limbs and tail are

expressed as funetions of the snout-vent length

(SVL). The range and mcum for cach form

is shown graphically in Figs, 14 and 15, Un-

fortunately, the sample size in some cases. is

extremely small because of the number of

specimens which had hroken tuils.

A general trend is. noticeable towards

shehtly relatively longer limbs and tails in

males (except perhaps in A. deeresii), While

there is wile overlap in the data of each form

amd the means of most of them approximate,

A. vadneppe stands out from the rest in its

greater mean relative length of both hind limbs

znd tail.

Femeral and preanal pores.

The total number of pores wax counted on

as Many specimens as possible, Unfortunately,

the pores on feihuale Ay decresié specimens were

so faint (especially distally) that teHable

counts could not be obtained.

The ranges und means of data for cach form

are shown graphically in Fig. 16. Wide over-

lap occut's in all forms with means of most

approximating. However, the Neplune Is.

sample is Outstanding in the telatively low

Means of both sexes.

The data represented in Figs. 14-16 reflect

the morphological uniformity of the complex

and confirm that pore counts and the telative

lengths of hind limbs and tail will nat serve

as useful characters for the recognition of «hE

ferent forms.

Discussion

Affinities af the vomplex

The A. deeresii complex shows obvious

uffinity with two other species: Aumphibolorns

rufescens Stirling & Zietz of north-western

South Australia and A. ornarity (Gray) of

south-western Australia, Both these species are

rock-dwellers agreeing with the diagnosis given

above for the 4, decresii camplex exeepr in

features of coloration, The adult mate of 4.

ofnatuy is boldly patterned dorsally with black

and yellow and the tail is banded. Sexual

dichromutism js not su pronounced in A.

rifescens as i A. ornares aT members of the

A. decresii complex: males tack bright colour

Washes about the lower jaw and throat but

are bright ferruginous dorsally, matching well

the colour of the rocks which thew inhabit,

These two species. and the A. derresil com-

pilex constitute a fairly well-defined and

Probably watural group which may be culled

the Amphikoluruy deeresil spectes-group.

Storr (1967) included 4. rufescens a3 a tace

of 4. caudicuictus (Giinther), a species com-

posed of several races distributed widely

throughout northern, central and north-western

Australia. I regard A. rufesceny as sufficiently

distinctive to merit specific rank but I do nat

dispute ite close wMinity with some races of A.

candicinetuy. It is quite probable that the

A. decresié species-group and 4. cundicincms

share u common ancestry,

Pigs. 1411, Amphihelvruy fionni. Adults in dorsal view. Fig. 10-—Holotype female from Pt. Lincoln

Area 4) Fiz. 11—Male

: from near Carrapateena Arp of Luke Torrens ¢Area 1).

Figs. 12-13, Amphibefuris vadnappe. Adults in dorsal

View, Fig. 12.—Tfolotype mute from Aroona

Waters (Area 6}, Fig. 13—-Male from Miriee Picnic Ground (Area 5)

58 T. F. HOUSTON

A. vadnappa

—_—__+—_——_.

A. fionni

| ——_—_+—____. ier

i N ———_}+—_—— 95

—__|——. 43

c ——_}———_. 14

———_}— io

Ww —__—___}———_ “eg

———_—_f>+—— sor

s ——+—. 1o¢9

—_|— 7o#

NI ——_}———_ 14%

A, decresii

A.vadnappa

A. fionni

A, decresii

Fig. 14. Hind limb length as a per cent of snout-

vent length in mature and near mature

individuals of the Amphibolurus decresii

complex. Ranges of variation represented

by horizontal lines and means by vertical

lines. Sex and sample size shown to right

of each. N = northern trace, C = cen-

tral race, W = West Coast populations,

S = southern race, NI = Neptune Ts.

race,

Tail length as a multiple of snout-vent

Jength in mature and near mature in-

dividuals of the Amphibolurus decresii

complex. Explanation as for Fig. 14.

Total number of femoral and preanal

pores in various forms of the Amphibo-

lurus decresii complex. Explanation as

in Fig. 14,

Fig. 15.

Fig. 16.

Superficially, at least, there is fairly close

resemblance between members of the A.

decresii species group and A. pictus which in-

habits chiefly sandy, shrub-dominated habitats.

Dispersal—past and present

Since the lizards of this complex appear to

inhabit only rock-strewn terrain, the question

arises as to how they could have colonized

the many isolated hills and ranges where they

now occur without haying crossed wide

expanses of soil plain.

While I have never seen adult and subadult

specimens anywhere other than amongst rock

REVISION OF THE AMPAIROLURUS DECRESH COMPLEX sq

Oulcrups, | have observed very small juveniles

vE A. decresif up to 100 oyetres away from the

nearest rocks uali\ohyst dense heath and une

Was observe’ wallowing in loose sand on 4

Ire path, This sugyests chat small juverriles

are get behaviourally tied to rocks as are older

uiimals and that some degree of dispersal over

non-rocky (efrain may be possible in the

juvenile stage, | would expect, however, that

the distances which such small tWards could

cover would be relatively small and pot

sufficient to explain the colonization of hills

separated by tens of kilometres of soil plain.

Because all members of the A. decresii

specics-group confine theniselves to rocky habi-

tats, I must assume that their ancesiors did ihe

same ind I believe they could have dispersed

ever long distances only where there Was suffi-

ciont rocky cover and where the gaps hetween

outcrops did not exceed the dispersal ability of

juyeniles,

It is Necessary to suppose, then, that rocky

terrain in past times was far more eatensive in

Sauth Australia than at present, providing

several cormdurs for dragon lizard dispersal

and that -crosion and deposition over very jong

periods eventually marooned many populations

as valleys widened and filled with alluvium.

I consider, too, that the lizards would not be

able 10 cross sea barriers in the wiy some

others ate able (such as by the rafling of

adults or their eges im Rood debris). The occur-

rence of members of the complex on several

islimds olf the coust of South Australia appears

to necessitale the assumption that the islands

were once part of the mainland and that ihe

lizards colonized them at that time.

Since the nearest living relatives of the A.

deerevé complex occur north and west of

South Australia, it is likely that ancestors of

the complex migtated in from those directions.

Migration is unlikely 10 have core through the

west ef the State where lies the Nullarbor Plain

and the sandy Great Victona Desert, or the

north-east Where lies the sandy Simpson

Desert. The only corridor which would have

heen available to ihe lizards lies between these

deserts and is constiluted by the Peake aad

Denison Ranges, Through these ranges the

lizards could have qmigroted from the Musgrave

and Everard Ranges, past the western side of

Lake Eyre tw the northern end of Lake Tor-

Tens.

This Jast inentidned lake and Spencer and

St. Vincent Gulfs lie in ihe prest, sediment:

filed South Austeuliun Rift Valley whact is

burdered along its eastern margin by the

Plinders-Mt, Lofty Range system and along

its Western Inargin by the Andamooka Ranges

and @ series of low ranges along the eastern

margin of Eyte Peninsula. Further migration

may then have occurred im two separate paths,

one each side of the sunklands. The eastern

path probably led them south to the area now

foluning Kangaroo {. and u branch could have

spread along the Olary Ridge {from Peter-

borough to the tegion of Broken Hill), The

western path may have led south to areas of

which the Neptune and Gambier Is. are now

remamants.

Expansion of the lizards’ range westwards

possibly occurred in two areas: (1) From the

hills near the junction of Lake Torrens and

Spencer Gulf through the Gawler Ranges sys-

lem as far west as Lake Everard, and (2) from

southern Eyre Peninsula north-westwards as

far as Nuyts Archipelago seross 4 great

expanse of seolianite (limestone) country.

While the latter expanse of rock does not

form any ranges, it does outcrop on low rises

and in gullies. It is not necessary to suppose

that this expanse was once exposed ulong the

full length of the West Coast to explain the

dragon lizards crossing it. Pockets of exposed

rack. as occur toduy, may have expanded,

coalesced, shjfted and shrunken with the pro-

cesses of crosion so that lizards may have been

able to move from one patch to another from

jime to time, gradually expanding thew range.

The limestone sheet surrounds many franitic,

eneissic and sandstone outcrops ahd prohithly

provided a pathway to them,

Evelution af races

T have sought below to fit the picture of

variation within the complex to the conven-

tional concept of new farms arising through

geographic isolation, although realleing that

alternative cxplanadions may be pdvanced.

Following colonization of major areas of

South Austraha by the ancestral form, changes

must have yqsen which rendered the ares north

of Lake Torrens unsuitable for habitation as

It now appears to be, Thus, populations of the

est were separated From those of the west hy

the Lake Torrens-Spencer Gulf sunklands. Per-

haps cuincident with these changes wos the

isolation of populations in the Northern Flin-

vers Runges from those further south, In this

hypothetical situatian we may envisage the

independent evolntion of the three main forms

found today-

fl) T. F. HOUSTON

ta) Anrphibolurus decresti

Because a single colour form occupies aTeas

on both Kangaroo J. and the southern Mt.

Lofty Ranges while another is found in the

more northerly ranges, it must be supposed

thal w& burrier to dispersal existed between the

North and South Mt. Lofty Ranges well betore

the separatian of Kangaroo J. by the forma-

tion of Backstairs Passage, The area now.

between Gawler and Kapunda, consists of very

low rolling hills which do not provide any

suitable autctops for habitation hy A. decresil.

The widening and filling of valleys between

individual ranges and hilly hus isolated many

populations in the more northerly parts of the

range of this species sind, presumably as a

result, a minor degree of diversity in colora-

Hon has arisen amongst them,

(b) A. flartm

The present distribution of male colour

forms sugeests isolation occurred of popula-

tions in Areas 1, 2, 3-4 (Fig. 1) and on Nep-

junc and Wedge Is. allowing genebc diver-

gence to develop,

Since the populations of Neptune and Wedge

Is, show strong differences from those of the

near mainland, it may be suggested that these

islands were separated (by the sea level rising

in telation to the and} much earlier than

islands to the north-west. where populations

appear more like those of the near mainland.

The generally deeper waters surrounding Nep-

tune and Wedge Is. give same credence tn this

theory. Huwever, It could also be sugaested

thar there are some differences in the habitats

occupied on these islands which exerted strong

selective pressures and brought about changes

in the inhabitants whereas the habitats of the

north-west islands were imuch the same as

those of the mainland,

Two barriers to dispersal must have arisen

another un southern Eyze Peninsula (isolating

area 2 from area 3-4). In these two areis

development of rocky Lerrait: was presumably

weaker than elsewhere 30 that the processes

of erosion and deposition were able to break

Jown or bury the rocks over a sufficrently wide

arca to disrupt dispersal.

As time went on, this process continued

within each area splitting off more and more

isolates. Even very small populations ry show

evidence of their jsolation. For example, an

unusually bold colour pattern characterises

females from the Marble Range.

{el A, yvadnappa

Only one major barrier to dispersal of this

species appears lo have arisen; a bread tract

of sandy country passing through Farina and

separating the Willouran Ranges from the

northern Flinders Ranges,

Perhaps subsequent to the formation of this

pap, the barrier separating 4. decresi/ from A.

vadnappa was overcome by the farnrer, thus

allowing colonization of the ensteta part of the

range of the Jatter. f am at a loss, however, to

sugvest just how this could have cone about,

The evolution of the A. decresi? complex, as

envisaged above, parallels the model of specia-

lion proposed by Pianku (1972) for habitat-

restricted livards Jiying in “shrub-Acecier! or

“sandplain-T'riodie" habitats. in both cuses.

habitats fluctuating in space and time are

helieved ta he the key factor.

Acknowledgements

The author is indebted to the many people

who provided specimens for the purposes of

this study, and who assisted him with collection,

in the field) Mr. R. W. Ellis, Curator of

Aboriginal and Historic Relics, South Austra-

lian Museum, kindly provided details of

on the mainland! one north-west of Pt. Aboriginal mythology connected with the new

Augusta (Separating area 1 from 2) and species.

References

Dumern, A. Mo Cc. & Brean, G. (1837).— Perers, E. (1864).—Obersicht der aus Buchsfelde

Erpétologic Générale ou Flisteire naturelle bei Adelside eingesandten Amphibien-

complete des reptiles, TV. {Paris.) Monatsh. Prenss. Akenl, Wiss, zu Berlin 1863,

228-234,

Dumus. A. M, C.. & Bron, G. (7834),—

Erpétologie Générale Athos, (Paris.

Fitzinger, L.,

(1843) —Systema

(Vienna.)

Keptilium,

Guint, J. (1954),—Catglogue des

Lézards du Museum National

Naturelle, (Paris,)

Types de

d'Alstoire

Pranka, B. R. {1972).—Zoogeography and speciu-

tion of Australian desert lizards: an ecologi-

cal perspective. Copeia 1972. (1), 127-145,

Procter, J. B. (1923)—On new and tare rep-

tiles and batrachians from the Australian

resins, Proc. zvol, Soc. Tond. 1923, 1069-

1077,

Sioxu, G. M. £1967),—Geographic races of the

agaoid lizard Amphtholurus caudicinetus, J.

R. Sar. West, Aust. 50(2), 49-56,

NOTES ON THE SMALL MAMMALS OF NORTH-EASTERN

SOUTH AUSTRALIA AND SOUTH-WESTERN QUEENSLAND

BY C. H. S. WATTS* AND HEATHER J. ASLIN*

Summary

WATTS, C. H.S., & ASLIN, Heather J. (19741.-Notes on the Small Mammals of North-eastern

South Australia and South-western Queensland. Trans. R. Soc. Aust. 98 (2), 61-69, 31 May, 1974.

The results of five field trips to north-eastern South Australia and south-western Queensland are

presented. The following four species (and numbers) of dasyurid marsupials were collected:

Sminthopsis crassicaudata (61), S. froggatti (3), Antechinomys spenceri (13), and Dasyuroides

byrnei (18). Seven species of native rodents were collected: Notomys alexis (3), N. cervinus (48),

N. fuscus (39), Pseudomys forresti (2), P. hermannsburgensis (8), P. australis (4), and

Rattus sordidus (many). In addition, a colony of Rabbit Bandicoots (Macrotis lagotis) was located

in Queensland.

NOTES ON THE SMALL MAMMALS OF NORTH-EASTERN

SOUTH AUSTRALIA AND SOUTH-WESTERN QUEENSLAND

by CH. S. Wartrs* aml HEATHER J. ASLIN*

Summary

Watts, C. H.S., & Asti, Heather J, (1974).—Notes on the Small Mammals of North-easlern

South Australia and South-western Queensland, Trans. R. Sec. Aust. 98 (2), 61-59,

3i May. 1974.

The results of five field trips to north-eastern South Australia and south-western Queens-

land ure presented, The following four species (and numbers} ef dasyurid marsupisis were

collected; Sminthops/y vrassicuudeia (61). 8. froygaitt (3), Antechinomys spenceri (13), and

Dasyaroides byrndi (18). Seven species of native rodents were collected: Netarnys alexis 13),

N, cervinus (48), No fuses (39), Pseudomys forresti (2), P. hermanisburgensis (8), P.

astealis (4), and Rattus sordidus (many). Tn addition, a colony of Rabbit Bandicoams

(Macrotis lagotis) was located in Queensland.

Distribution, status, and habitat preference within the avea is discussed for 9 number of

species collected. In particular, R. sordidtis was found to be common in 1968 and 1972, but

micommon in 1971, when it was restricted to wet areas around bores and floodplains, Lt is

suguested that, following periods of good rainfall, R. serdiduy spreads from mesic refuges and

temporarily occupies surrounding areas, giving rise to plagues in exceptional years,

Introduction

Knowledge of the distribution and habits of

many of Australia's small desert mammals is

accumulating only very slowly. There is litile

or no published information on many species

of native rodents and small marsupials from

the central areas of the continent. Without

further distributional cecords it is impossible

lo assess whether these species are maintaining

ther numbers, or have been striaysby affected

by land-ase practices and by the presence of

exotic mammals,

In the hope of adding to present knowledge

of the distribution and habits of smali desert

mammals, this paper reports the findings of

five field trips to north-eastern South Australia

and suuth-western Queensland. The ficld work

wits Carried out with the aim of collecting small

mammals to establish breeding colonies in cap-

livity, However, in the course of this work.

information was Obtained on the distrilnition,

status, habitat prefercnce, .and hahits of the

species collected. This information is a neéces-

sary prerequisite for effective conservation of

the various species in the wild.

The species collected were the following: the

dasyurid marsupials Sminthopsis crassiceudata,

S. froggaui, Dasyweoides byrnet, and Ante-

chinomiys spenceri; the rodents Natomys alexis,

N, cervinus, N. fuscus, Pseudamys australis, P.

hermannsburgensis, P. forresti, and Rattus sor-

didus. Information was also obtained about the

status of the Rabbit Bandicoot (Macroris

lagolis) in Queensland. A representative speci-

men of each species collected has been lodged

in the South Australian Museum,

Methods

Five trips were made, in September 1968,

June 1969, June-July 1971, July 1972 and

October 1972. A total of 43 days was spent in

the field. A summary of routes taken is shown

in Fig. |,

Most animals were caught by spot-lighting

on 33 nights, usually between the hours of

20.00 to 24.00, After detection, animals were

caught in a hand-held net. Sherman live mam-

mal traps (7 x 8 x 23 cm) were set on several

occasions. Two species were obtained by

digging up. burrows.

Some animals were released after examina-

tion, but imost were transported to the labora-

tury alive.

As it was difficult 10 determine precise loca-

trons at which animals were caught, the Joca-

tions given are approximate.

7 Institute of Medical und Veterinary Science, Frome Road, Adelaide, 5, Aust. 5000.

62 c. H. S. WATTS & H. J. ASLIN

GLENORMISTON 14

0°

HS ee RBOULIA

MARION

DOWNS Hs: COORABULKA

H.S

SANDRINGHAM) HSm_/ |

BEDOURIET | \ OLD

GLENGYLE® J &MONKIRA

H.-S. 1¢ \ HS.

DUR DIE HS JaeTOoTA

BIRDSVILLE,

J HS. CORDILLO DOWNS

H.S.

INNAMINCKA

H. S.

M\MULKA /

H.8.

‘ /

Q /

NE mE ARR EEN

} Z

aed

ADELAIDE

KILOMETRES

135

Fig. 1. Summary of the routes taken on the five field trips. The routes followed are indicated by a

broken line,

CHANNEL COUNTRY MAMMALS 63

Nomenclature used in this paper follows that

of Ride (1970), with the exception of the

Long-haired Rat, which is now considered by

Taylor & Horner (1973) to be a subspecies

of the Dusky Field-rat, and is therefore

referred to as Rattus sordidus villosissimus, not

Rattus villosissimus.

Results

MARSUPIALIA

Family PERAMELIDAE

1. Macrotis lagotis (Reid), Rabbit Bandicoot

Locality: 16 km N Coorabulka Homestead, Qld;

July 1972; 1 (sex unknown).

Notes; One Rabbit Bandicoot was sighted on

gibber plain while spot-lighting, and this ani-

mal took refuge in a complex burrow system,

consisting of approximately 20 holes, Reports

from local residents indicate that a colony of

M. lagotis exists in an area extending from

Coorabulka Station into the adjoining stations

of Marion Downs and Lorna Downs.

In addition to this colony. reports of ani-

mals answering the description of Rabbit Ban-

dicoots were obtained from residents of Glen-

gvle and Sandringham Stations.

Family DASYURIDAE

|, Sminthopsis crassicaudata (Gould),

tailed Dunnart

Fat-

Localities: (() 72 km NE Anna Creek Homestead,

S.A.; Tune 1971; 2 @. (ii) 8 km E Mulka Home-

stead, S.A.; June 1969, July 1972; 2 ¢. (iii) 112

km SW Innamincka Homestead, S.A.: June 1969:

1 9. (iv) 80 km N Innamincka Homestead, S.A.;

June 1969; 1 9, 1 & (v) 8&8 km § of Birdsville,

Qld: Sept. 1968, June 1969, Oct, 1972; 4 9, 12 2.

(vi) 48 km SE Pandie Pandie Homestead, S.A,:

July 1972: 1 9. (vii) 16 km W Betoota, Qld: June

1969, July 1972; 5 &. (viii) 32 km W Durrie

Homestead, Qld; July 1972; 1 ?. (ix) 32 km NW

Monkira Homestead, Qld; July 1972; 1 &. (x) 16

km W Corrabulka Homestead, Qld: July 1972: 8

3. (xi) 32 km NW Coorabulka Homestead. Qld:

July 1972; 1 2 (xii) 16 km N Coorabulka Home-

stead, Qld: July 1971, July 1972; 5 2. (xiii) 8 km

SE Sandringham Homestead, Qld: Sept. 1968:

female with three young. (xiv) 8 km S$ Glengyle

Homestead, Qld; Sept. 1968; 2 9, 9 d. (xv) 8 km

E Glenormiston Homestead, Qld; Sept. 1968; 1 ¢.

Notes: S. crassicaudata was found in a variety

of habitats, including gibber and sand plain,

alluvial flats, and clay pans. One animal was

trapped by a bore drain, The species appeared

to be thinly spread in most areas, but 11 ani-

mals were caught by spot-lighting in an area

of less than 2 hectares near Glengyle Home-

stead, on recently flooded clay pans.

2. Sminthopsis froggatti

faced Dunnart

Localities: (i) 16 km N Pandie Pandie Homestead.

S.A.; Sept. 1969: 1 & (ii) 16 km N Coorabulka

(Ramsay), Stripe-

a : ee

ee i ne

BR yy

Soe 5 >

Fig. 2. Habitat of Sminthopsis froggatti on Coorabulka Station, Qld.

64 Cc. H. 8S. WATTS & i. J.

ASLIN

ig. 3,

Homestead, Qld: July 1972; 1 ¢, (iii) 32 km NW

Coorabulka Homestead, Qld; July 1972; 1 ¢.

Notes: One of the three S. froggarti is illustra-

ted in Fig. 3. together with the habitat in

which it was collected.

3. Antechinomys

wuhl

Localities: (i) & km W Birdsville, Qld; July 1969;

1 &. Gi) 16 km W Betoota, Qld; June 1969, July

1972, Oct. 1972; 3 @, 5 &. (iit) 16 km W Coora-

bulka Homestead, Qld; Sept. 1968, July 1971,

July 1972; 2 9, 2 ¢.

Noies: A. spenceri was captured on gibber

plain, by spot-lighting, and at each of the three

localities was sympatric with the rodent,

Notomys cervinus. One female A. spencert

took refuge in what appeared to be a disused

burrow of N. cervinus.

spenceri Thomas, Wuhl-

4, Dasyuroides byrnei Spencer, Kowari

Localities: (4) 8 km SE Coorabulka Homestead,

Qld; Sept. 1968; 1 9. (ii) 16 km N Coorabulka

Homestead, Qld; July 1971; 8 9, 6 &. (iii) 16

km W. Coorabulka Homestead, Qld; July 1971;

2 4 (iv) 8 km N Coorabulka Homestead, Qld;

July 1972; 1 2.

Notes: Of the 18 animals collected, 14 were

trapped, two were caught by spot-lighting, and

one was a road-kill.

Adult male S. froggatti from Coot

een

rabulka, Old,

In July 1972, seven D. byrnet were sighted

on station roads north of Coorabulka Home-

stead. When pursued, two of these animals

took refuge in burrows occupied by Long-

haired Rats (R. s. villosissimus) which were

abundant at the time. All D. byrnei were cap-

tured on gibber plain.

Reports of animals which may have been

D, byrnei were obtained at Betoota, Qld, and

a skull of D. byrnei was found under an air-

port marker near Betoota.

RODENTIA

Family MURIDAE

1. Notomys alexis Thomas, Spinifex Hopping-

mouse

Localities: (i) 80 km N Innamincka Homestead,

S.A.; June 1969; 2 d. (ii) 8 km SE Sandringham

Homestead, Qld; Sept. 1968; 1 3

2. Notomys cervinus (Gould), Fawn Hopping-

mouse

Localities: (i) 48 km S Pandie Pandie Homestead,

S.A.: July 1972; 1 2. ii) & km S Birdsville, Qld;

June 1969: 1 9, 2 &. (iii) 16 km N Birdsville,

Qld; Sept, 1968; 3 9, 13 ¢. (iv) 16 km W Betoota,

Qld; June 1969, July 1972, Oct, 1972; 3 9, 3 ¢.

(v) 32 km W Durrie Homestead, Qld; July 1972;

2 9 (vi) 16 km S Glengyle Homestead, Qld;

CHANNEL COUNTRY MAMMALS 65

Sepl, 1968: 5% 9 ¢, tvii} 16 km § Glengyle

Homestead, Qld; July 1971, | 9, 4 dt. évili) 16

km N Cocrabwka Homestead, Qld; July 1972; 12

Notes; A total of 15 Females aiid 31 males of

N, cenvinus were captired, hy Spot-lighting,

either on open gibber plain, ov gibber Plain

with alluvial flats. Several WN, cervinis took

Tefuge in burrows which oonsisted of one to

three closely grouped entrance holes, situated

on open gibher plain.

3. Notumys fuseus (Jones), Dusky Hopping-

mouse

Loenlities: (i) 16 km N Birdsville. Qld; Sept.

1968; 1 of. (ii) 16 km W Betoola, Qld; Jime 1969,

July 1972, Det. 1972; 2t 9. 17 A’

Netex: All N. fuscus from Betoota were ob-

tained from a limited area of sand ridge which

wis visited on four occasions (Fig. 4).

Two burrow systems of NV. jascur Were exca-

vated, and a diagram of one is shown in Fig

6, Neither of the burrows contained animals.

4. Psendomys forresti (Thomas), Forrest's

Mouse

Localities: (t) 16 km W Coorabulka Homestend,

Qld; July (972; 1 &. (ii) 32 km NW Coorubulka

Homestead, Qld; July 1972: 1 2,

5. Pseudomys (Leggadina) hermannsburgensis

(Waite), Sandy Inland Mouse

facdites: (i) 8 km SE Sandringham Homestead,

Qid; Sept. 1968: 1 2 (fi) 16 km W Betoota, Qld;

June 1969, July 1972, Oct. 1972; 7 3, 3 ot (iii)

ea km aw Coorabulka Homestead, Qld; July

S721 ds

6. Pseudomys australis Gray, Plains Rat

Lacaiit\; 96 km NE Cardillo Downs Nomestead,

S.Au June 1969; 3 9. 1

Notes, the four 1, aristralis were obtained from

a-single burrow, Which was one in an exten-

sive area of burrows situated on gibber plain

with clay-pans. Seven burrows were dug Up.

hut only che was occupled. Sections of some

burrows were stuffed with green vegetation,

7, Rattus sordidus villosissimus (Waite), Long-

haired Rat

Localities; Li) 16 km N Clifton Hits Homestead,

S.A; Sept. 1968; 3 2 5 3. (ii) 32 km NE Clifton

Hills Homestead, S.A; Sept, £968; 7 9, 1 @. ili}

{6 km N_ Birdsville, Qld; Sept. 1968, July 1971;

99, 11 a Civ) 72 km NE Anna Creek Home-

stead, S.A.; June 1971; 2.9, 1 co. tv) 32 km SE

Pandie Pandie Homestead, 5A. July 1971; ) ¢

und 6 young. | do. (vi) 16 km N Coorabulka

Homestead, Qld; July 1972; many animals,

Notes: Sixteea R. 5. villorissimus were trapped

On sand-ndges and flood-plain at Clifton Hills

Station in 1968. Green vegetation was plentiful

at this time, A further 20 animals were trapped

sear Birdsville on pibber plain in 1968 and

1971.

The loculity on Anna Creek Station was a

rord ahd sedge area around a bore drain, while

on Pandie Pandie Station a female and her six

young were dug out from a simple burrow in a

sand ridge close to flood-plsin. The young

were enclosed in a spherical nest of shredded

plant material.

In July 1972, signs of R, s. villosissimus

were found in most areas visited, from’ Mulka

Station northwards. Many rats were sighted

during sporighting on Pandie Pandie, Durric,

Monkira and Coorabulka Stations, and also

near Betoota. They Were in plague proportions

on Coorabulka Station, where many were

trapped on gibber plain, and extended north

to Boulia.

Discussion

The finding of Macrotis fagotis in south.

western Queensland js of interest because of

its present rurity and great decrease in range

this century, Mack (1961) obtained Rabbit

Bundicoots from near Birdsville in 1957-59,

but the species has not heen seen recently in

this area. Smyth & Philpott (1967) found the

species to be common at Warburton Mission,

W.A., and Walls (1969) focated colonies at

¥Yuendumu, Hamilton Downs and Papunya in

the Nosthern Territory, This study suggests

that Rabbit Bandicoots may still occur in

scveral areas of western Queensland, where

rabbits and foxes are in low numbers.

OF the four species of dasvurid marsupials

collected, Smikihopsir crasticaudata was the

most common, and appears to occur fn all

types of hahitat in the area studied, S$. cresyi-

caudata from these areas were characterized by

larger ears, Jonger tails and paler cost colour

than animals from southern South Australia,

and are relercable to the sub-species S. crarsi-

caudata ventralis Thomas,

Another species of Siminthopsix, identified

by M. Archer (pers. comm.) as S. froggatri

(sens. Ride 1970). was obtained jn the same

areas as 3 crassteaudata, but was much less

common.

Ag extremely biassed sex ratio of 46 males

tot] females (four animals were pot sexed),

was found for S. crassicaudata capmted by

spotlighting. This contrasts with Wood Jones’

(1923) finding that many more fernales than

males Were captured by trapping and by

domestic cats, This serves ro illustrate the way

46 C,H S. WATTS & H. J. ASLIN

in which methods of capture may discriminate

avainst one sex in Favotr of the other,

OF the 11 female S. crasstcaudafa captured,

mindy two hud young, beth in the spring manths.

Since ull animals were captured in winter ur

spring, and since most breeding in 5. crasi-

cadate occurs between July and February, both

it the field and in the luboratory (Godfrey &

Crawernft 1971), it is surprising that more

females with young were not captured. It

seems that cither only a small percentage of

females are breeding wl any one time, or that

methods of capture which depend on the

amount of time which the animals spends

aclive outside refuges discriminate against

females with pouch young. This is consistent.

with Ewer’s (1968) observations. that captive

females with pouch young were Jess active

than usual,

The small dasyurid Antechinombs spéencert

was found to be moderately common in several

areas of southewestern Queensland, but Was

fot taken in South Australia, and appears to

be rare in the north-east of the State, although

Finlayson (1961) found it plentiful in the

Everard and Musgrave Ranges of the north.

west. All the animals captured in Queensland

were taken on gibber plain. which contrasts

with Wood Joncs' (1923) statement that A,

ypeneer’ is an animal of sand-tidge desert.

Marlow (1968) also found A, spenceri in ateas

of gibber plain habitat,

Until recently A. spencer? was believed to

hop bipedully like the munds of the genus

Notomys. Ride (1965) showed, however. thal

A. spencer’ moves quadrupedally at all times.

and Marlow (1968) found thal A. spenceri

wiso adopted different escape lactics from N

cervirus when pursued | similar habitat. This

was also noted in the present study, A- spencer

frequently crouched behind small clumps of

vegetation, relying on concealment to escape

capture, whereas NV. cervinws invariably hopped

at high speed. and frequently changed uirec-

lion,

Unfortunately none of the female A. spen-

cert from Queenslund had pouch young,

although there is a tecofd of one fernale with

young which was captured in September in

the Northern Territory (unpublished data). If

this species breeds during the winter and

spring months, once again it is surprising that

none of the five females captured had pouch

young, The argument used fe account for the

similar situation wit) §. ¢rassicaudata may NOt

he applicable Io A. spenceri, vs only 3 slight

excess Of males (8 males, S females) was te-

corded for this species,

Dasyuroides byrnei was found in a Jimited

ea OF south-western Queensland, and appears

to be restricted to gibber plain, The type

juculity of rhis species is Charlotte Waters an

the Northern Terntury, and it has been taken

ax far south as Killalpaninna, on Coopet's

Creek in South Australia (Wood Jones 1923),

However, D. byrne? has seldom been collected

trom the Northern Territory or South Aus-

iralia in recent times, although it remaims com-

mon |i parts of south-western Queensland,

Seven of the eight female D. byrnei collected

its July. 197), had pouch young, all of which

were estimated ie have been hor in June,

Woolley (1971) collected = pouch-gravid

females in June, and pregnant females in

November. Female cycles appear to be syn-

chronized in this species, and most females

come into breeding condition in May or Junc

both in the ficld and an the laboratory.

Turning to the rodents, firstly it is worth

noting that although seven species of native

todents were collected, the introdyced house

mouse (Afus mmuscafus) was not found in the

grea under study, Of the native rodents ob-

tained, Neroneys cervinus was the most com-

mon: 48 were collected in South Australia and

Queensland. N. cervinus was found on both

gibber plain and alluviai flats, bue not on

sandy areas, It was abundant in some paris,

particularly near Betoota. N. cervinas appears

10 be a soctal species as indicated by the

groups of thres to four animals sighted simul-

tancously in the field.

Of the 15 female N. ceryinus collected, one

Wag lactating in September, and another preg-

nant in July, One juvenile was also collected

in July. These records suggest that N, cervinus

muy be a winter breeder im the wild.

Noromys fuscus was obtained at Betouts in

the same tinea as NL cervinus, which it closely

resembles. However, hoth sexes of N. furcus

have an abvious gular pouch, which distin-=

guishes the species from N. cervinus, in which

neither sex possesses a gular pouch (Aitken

1963).

N, fuscus was found to be abundant on one

sunc-ridge near Betoota, and was apparently

confined to this ridge. N. cervime was collec-

ted from the adjacent gibber flats, but only

one WN. fasciry was captured on these flats. Ie

seemed, therefore, that N. fascws ventured

only rarely onto open gibber plain. Aitken

(1968) has mapped the distribution of N-

CHANNEL COUNTRY MAMMALS

GROUND

MAIN TUNNEL

Fig. 4. Habitat of Notomys fuscus near Betoota, Qld.

Fig. 5. Adult female N. fuscus.

Fig. 6.

Diagram of a burrow system of N. fuscus excavated on the sand-ridge shown in Fig. 4.

ns CHS WATIS & HJ

liven, ad has shown thal most records ot

this species are from north-eastern South Aus-

tralia, With the greufest concentration between

Lake Eyre and the Queenshind border The

present record fronr Betoata appears to be the

most northerly locality al which the species

hus been tuken.

Burraws of No fayvedy located on the sanil-

ridge conformed ty the typical Naroinys pat

tern (Fig, 6), baving several vertical shafts

descending te a depth of 70-140 cm (we to

four feet), The number of animuls present on

the Sanmteridge appears to fluctuate, as none

was sighted in June. 1971, although conditions

at this time were better than in July, 1972,

when No fivens was eoninian. In addition, two

females collected in July, (972, were pregnant,

one gave birth to fiye young within a week of

cupture. vod the other wave birth to one young

33 days uffer capture. Breeding in this species,

if opportunistic us suggested for many desert

rodents, may not be directly dependent on

rainfall, ar there may be a considerable lag in

response to improved conditions. Watts

(1970) has shown that NV. fliserns eats mainly

seed in the wild, and much af this seed may he

lost cue to germination immediately after

counfall,

A lhed Navainy species, No alexis, Was col-

jected from) two areas Of sand-pluin covered

with Triedia, but was not common in the areas

Visited. From these records it can be seen that

the three species of Nerteniys in south-western

Queensland have distinct habuut preferences:

N, cervinus favours open gibher or alluvial

plains, No fesers intuthits sarudi-ridges, und Vy,

dleviy lives ou the furter ureas of deep sand.

Three species of the genus Preadomry were

collected: PF. fortes, Po heriannshargensisy

and P. astreliv, The reeords of Po lermanns-

burgdnséy from Queensland are unusiull, as the

greqlest concentration of thix speectes is to the

west of Alice Springs, some 480 km front the

present loealities, Finlayson (1961) states that

he could obtain na evidence of this species to

the east of Stuart's Line, hut in this study P,

hermuannsburgensiv owas taken from three

widely separated localities in western Queens-

Lamel.

Of the four female P. heridnishireensis

captured, one was pregnant when collected in

June. 1969. and pave hirth to two young eight

duys after capture. One juvenile male was

collected in July, 1972, indicating that this

species shows breeding activity in the winter

months, Similarly, Wwo of the three female P-

ASTIN

australiy collected in June, 1969, were preg-

nant, and gaye birth to three and two young

in the laboratery at 15 and 16 days alter ep

fure.

Raitas sordidaus vitlosissonus was callected

vn muiny Occasions, and some conclusions

about its habits can be drawn, This species is

known fo intrease vastly in mumbers at inter-

vals of five to seven years. und Finlayson

(1961) suggested that at these times Tt swarms

from a breeding centre in western Queenslund

into South Australia and the Northern Terri-

tory. This theory requires large-scale migration

of the species into previously unoccupied areas,

Information from the present study indi.

cules (hal dtirigg rat plagues the animals can

be found in-all types of habilul, provided green

phints of roots are available as a source of

vuter, as Roy. villosissiuaty ts unable to stir

vive without preformed water (unpublished

data), These conditions prevailed in 1968 ani

972. When the species was abundant from

northern South Australia to Boultu in Queens-

lund. However, animals collected in 97) were

obtained from areas close lo water, Such us

uround bore-drains and from flood-plain

Three females obtained fram Cliflan Hills

Station in L9O8 were pregnant, bur there was

evidence thal the vals were decreasing (ew

range in this area. us there were muny unoecu-

pied burrows in gibber plain) whieh had

recently dried out, In a good segson it seems

that Ry s. villosisvintny can occupy all pes of

habitat, hut as vegetation dries oul the gibber

plains are the first areas which became un-

tenable. Similarly, in 1972, although ruts were

present on gibber plat in many areas, they

were most numerous around bore-trains. and

animals living on the open pluins were often

in poor condition,

This information suggests that R. 9 villosis-

sims ig always present in small numbers 1

pockely of favourable habitat. such as around

bore-deains. In sueh pockets the rats can sur-

vive droughts, and if conditions improve in

surrounding ureas they are able to expand inte

these ureas, These successive expansions from

many breeding ouclei are therefore responsible

for rat plagues, nut mgss migration from a

single centre in westem Queenskind, In mesic

refliges R, », villosivsinnis 8 a relatively eryptie

species. which may account for the common

helieF that it is completely absent from most

areas in non-plague vears-

In summary, it seems that a number of

native mammals are moderately common in

CHANNEL COUNTRY MAMMALS f9

nosth-eastern South Australia und south-

western Queensland, in spite of almose com-

plete pastoral exploitation of the area, The

small mammals have fared better than those

of intermediate size. In purticular, the desert

bandicoots have suffered greatly in this cen-

tury. Macrotis leticura, Chaerapus ecaudatur,

Perameles eremiana and lsoodon atiratus all

appear to have vanished with the invasion of

the fox inte central Australia ( Finlayson

(961). In view of this fact, the Rabbit Bundi-

coot is most urgently in need of protection in

Queenslund, as the colonies in this area are

probably small and are widely separated from

other known colonies,

Many of the small mammals, however,

uppear to be maintaining their numbers,

although in many cases little is known about

their distribution and habits. This lack of

knowledge can only be remedied by more ex-

tensive field work carried out regularly ovet

long petiods. Such field work is particularly

necessary for an understanding of the popu-

lution dynumics of many of Austealia’s native

rodents.

Acknowledgements

We are perateful to the Department of

Fisheries and Fauna Conservation, South Aus-

tralia, and the Department of Primary Indus-

tres, Queensland, for allowing us to collect

small mammals in the two States, and for

issuing the necessary import arid eXport per-

mits,

The following people carried out field work

it various times: Mr. C. Hann, Mr. J, Harlow,

Dr. Ci, Judson, Mr. C, Pettet, Miss A. Olner,

Mr, J. Satchell and Mrs. G, Watls. We ate

extremely grateful for their assistance in what

was often exhausting work. We appreciate the

advice of Dr, M. Archer of the Queensland

Museum on the identification of Sminhopsis

specimens,

Thanks are also due to the residents of a

number of stations, particularly Coorabulka

Station, for helpful adyice and assistance,

Finally, we must thank Dr. P, S, Watts,

whose interest and encourayement made this

work possible,

References

AITKEN, P. F. (1968).—-Observations on Notomys

fuseus (Wood Jones) (Muridae-Pseudo-

mylnae) with notes on a new synonym. S.

Aust. Nat, 43, 37-45.

Ewer. R. F. (1968),—A preliminary study of the

behaviour in captivity of the dasyurnl mar-

supial, Sminthopsts crassicaudara (Gould),

Z, Tierpsyvhol, 25, 319-365,

Fintayson, H. H. (1962).—On central Australian

mammals. Part IW—The distribution and

status of central Australian species, Rec. S.

Aust. Mrs, 14 (1), 141-191.

Goprrey. G. K,, & Crowcrorr, P. (1971).—

Breeding the Fat-tailed marsupial mouse in

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South = Australia”. (Government Printer:

Adelaide, )

Mack, G, (1961)—Mammats from sonth-western

Queensland, Mem, Old Mus. 13, 213-229,

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locomotion of two desert-living Australian

mammals, Atfechinomys spenceri (Mar-

zupialias Dasyuridae) and Notomeys certnus

Peouenba: Muridae). J. Zoni., Lond. 157,

Putyporr, C, M.. & Smyrn, D. R. (1967)—A

contribution to our knowledge of some rare

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Rink, BD. L, (1965)—Lacomotion in the

Australizn marsupial Antechitobiyys. Nature

205, 199,

Rive, W. D. L. (1970) —"A Guide to the Native

Mammals of Australia”. (Oxford University

Press: Melbourne.)

Smytn, DR, & Purrrporr, C. M. (1968).—A

field study of the rabbit bandicoot,, Macretiz

lugotis, Marsupialia, from central Western

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TayLox, J. Mary, & Horner, B:. ELizaperu

(1973),—Results of the Archbold Expedi-

tions. No. 98, Systematics of native Austra-

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Mus. Nat, fis. 150, 1-130.

Watrs. C. H. & (1969).—Distributlon and habits

of the rabbit bandicoot, Trans, R, Spe. S.

Asi. 93, 135-141,

Warts. C, H. S. (1970),—The foods eaten hy

some Australian desert rodents. S Aust, Nat,

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NEW SPECIES OF HYLID AND LEPTODACTYLID FROGS FROM

SOUTHERN NEW GUINEA

BY M. J. TYLER* AND F. PARKER

Summary

TYLER, M. J., & PARKER, F. (1974).-New Species of Hylid and Leptodactylid Frogs from

southern New Guinea. Trans. R. Soc. S. Aust. 98 (2), 71-77, 31 May, 1974.

Two new species of frogs (a hylid and a leptodactylid) from southern New Guinea are described.

Details of habitats and habits are provided, and an analysis of the mating call of the leptodactylid is

included.

NEW SPECIES OF HYLID AND LEPTODACTYLID FROGS

FROM SOUTHERN NEW GUINEA

by M. J. TyLtea* and F. Parkery

Summary

Iycer, M, J, & PARKER, F. (1974).—New Species of Hylid and Leptodactylid Frogs {rom

southern New Guinea. Trans. R, Soc, 5. Aust, 98 (2), 71-77, 31 May, 1974.

Two new species of frogs (a hylid and a leptodactylid) from southern New Guitiea are

described, Details of habitats and habits sre provided, and an analysis of the mating call of

the leptodactylid is included.

introduction

In @ recent comparigon of the Australian

and Papuan frog faunas adjacent to Torres

Strait, Tyler (1972a) indicated that few

species are exclusiye to the Papuan ccastal

urea. However, it was noted that literature

references to the occurrence there of the Aus-

tralian leptodactylid Crinia signifera (Roux

1920; Van Kampen 1923; Parker 1940) ante-

dated knowledge of the existence of a com-

plex of species previously so identified (Moore

1954. Main 1957), and probably represented

an wndesceribed species,

Tyler & Parker (1972) increased the known

Papuan hyhd frog fauna by describing Litoria

ltmida from the upper tributaries of the Ply

River, and from localities situated closer to the

coust in the south-east of Papua New Guinea-

On 4 March, 1973, one of us (F.P.) collec-

ied vight species of frogs at Merauke, situated

only 80 km west of the area from which the

collections of Tyler & Parker (1972} were

obtained. One of these species reptesents a

previously undescribed hylid which we des-

cribe here. Moreover, we now have adequate

material from previous collections in southern

New Guinea to re-examine the taxonomic

status of the leptodactytid,

Crinig Tschudi, as recognised by Parker

(1940), is now regarded as constituting four

dislinet genera: Assa Tyler, Crinia Tschudi,

Geacrinia Blake and Ranidella Girard (Tyler

1972b; Blake 1973). The Crinia signifera com-

plex has been referred to Runidella by Blake.

und the species that we describe here is » mem-

ber of that genus,

Methods

The specimens discussed here are deposited

in the collections of institutions abbreviated in

the text as follows: American Museum of

Natural History (AMNH); Museum of Com-

parative Zoology (MCZ), Naturhistorisches

Museum Basel (NMB): South Australian

Museum (SAM), and Department of Biology,

University of Papua New Guinea (UPNG).

The methods of measurement and morpho-

logicul and descriptive terminology follow

those of Tyler (1968). The descriptive abbre-

viations used are: E (horizontal diameter of

the eye); E-N (distance between the eye and

the naris); IN (Ginternarial span); HL (head

length); HW (head width); S-V (snout to

vent length); and TL, (tibia length). Tech-

niques of call recording and analysis follow

Tyler & Menzies (1971).

Merauke is situated approximately 80 km

west, Gubam 30 kn east, and Mata 10 km

east, of Morchead (Tyler & Parker 1972, Fig.

1).

Litoria quadrilineata n.sp,

Holotype: SAM R13489, An adult male

collected on Jand adjacent to the Post Office,

Jalan Trikora (—Trikora Road), at Merauke,

Irian Jaya (formerly West Irian), New

Guinea, by F. Parker on 4 March, 1973.

Definition; A small lowland species (males

27,4-30.5 mm S-V) characterised by a narrow

* South Australian Museum, North Terrace, Adelaide, S. Aust. S000.

t Wildlife Section, Dept. of Agriculture Stock and Fisheries, Konedobu, Papua New Guinea

“+

Fig, 1, Hand and foot of Eitorie guadrilineuta.

and rather clongated head und body. short

limbs, unwebbed fingers, vestigially webbed

toes and four dark, longitudinal stripes on the

lateral and dorsal surfaces of the body.

Description of Holetype; The head is high,

triangular when viewed from above, and banger

than broad (HL/HW 1,089), its length equiva-

lent to slightly more than one-third of the

snout fo vent length. The snout is high and

prominent when viewed from above, rounded

and projecting beyond the anterior limit of

the mandible in profile. The nostrils are situa-

led laleratly, their distance from the end of

the snout being approximately one-half that

from the anterior margin of the eye. The dis-

tanec between the eye and the aris is greater

thin the internarial span (E-N/TN 1.083),

The canthus rosttalis is of moderale length,

clearly defined and very slightly curved, whilst

the loreal region is markedly concave, The eye

is of moderate size and not conspicuously

prominent, its diameter equivalent to the dis-

lance between the eye and the naris. The

tympanum ey conspicuous, with a narrow annu-

jus partly hidden superiorly by a supra-tym-

panic fold, The tympanic diameter is equiva-

lent to approximately one-half of the horizon-

tal diameter of the eye. Vomerine teeth are

absent: there is a slightly raised clevation on

the left side but not on the right. This eleva-

tion is situated between the chononae, The

tongue is broadly oval with a very weak pos-

tenor indentahem-

M.. TYLER & F, PARKER

The fingers are tong, slender, unwebbed, and

possess Only extremely slender lateral Iringes

(Fig. 1), The decreasing order of length of

the fingers is 3>452>1, The terminal discs

are moderate, the diameter of the discs of the

third finger being approximately one and one-

half times the diameter of the penultimate

phalanx,

The hind limbs ure relatively short and

slender, with a TL/S-V ratio of 0.407, and

lucy in decreasing order of length 4>3>3>2 =

1. Only a vestigial trace of webbing occurs

hetween the fourth and the fifth, and third

and fourth digits (Fig. 1). There is a small

circular inner but no outer metatarsal tubercle.

The dorsal surfaces of the head, body und

limbs ate minutely granular, Distinct tubercles

are lacking. The skin of the throat and chest

Jacks tubercles, but is greatly folded and con-

voluted in association with the vocul sac. und

is clearly a reflection of the calling activity of

the specimen prior to preservation, The abdo-

men und ventral surfaces of the femora are

granular, There is an extremely prominent

gland at the post-articular mutgins of the man-

dibles,

This. male specimen has w large, single sib-

mandibular vocal sac with longitudinal puired

apertures bounded by the anterior cornua, and

glandular but completely unpigmented nuptial

pads,

The dorsum is a very pale brown, on which

there are four narrow, bul conspicuous, longi-

tudinal black stripes. The median pair com-

mences on a Jevel with the anterior margins of

the upper cyelids and extends to the femora.

The lateral stipes extend from the tip of the

snout to the inguinal region, In addition there

is a very natrow and much less conspicuous

mid-vertebral stripe, and a pair of short dark

stripes on cach side of the cloaca, extending

to a position anterior to the level of the

femora. “There is a dark stripe on the outer

margin of the forearm anda pair of mare con-

spreuous dark stripes on the dorsal surface of

the tibia and the tarsus, The post-labial gland

is white and the venital surfaces of the body

and limbs are dull cream and immaculate.

Dimensions: Snout ta yent length 29,9 mm:

tibia length 12.2 mm; bead length, 9.5 mm;

head width 8.6 mm; eye to maris distance 2.6

mm} internarial span 2.3 mm; eye diameter 3.1

mm; tympanum diameter 1.9 mm.

\arlation; The paratype series. consists of

twelve adult males (MCZ 86014-21, SAM

R13480-93}, collected jt Merauke with the

NEW SPECIES OF NEW GUINEA FROGS 73

Fig. 2. Litoria quadrilineata in posed position shortly after preservation,

holotype. They differ only slightly in size, the

snout to vent length range being 27.1-30.0

mm, with a mean of 28.8 mm. The limbs are

consistently very short (TL/S-V ratio 0.39-

0.44) and the body slender. The HL/HW

range is 1,100-1.143 and the E-N/IN range

1.125-1.182. Figure 2 is of a freshly killed

specimen in a posed position.

Vomerine teeth are present on distinctly

raised vomerine elevations; the vomerine eleva-

tions may be present and teeth absent or both

elevations and teeth entirely absent.

The post-labial gland is present and con-

spicuous in ten paratypes but is entirely lack-

ing in two, Although all specimens have the

skin of the throat gently convoluted and folded,

indicating a period of prolonged vocal activity

prior to collection, the nuptial pads are unpig-

mented.

In preservative the four longitudinal stripes

are present throughout the series, the speci-

mens differing only slightly in the background

coloration: some being dark brown and

others a sandy brown,

The description of colour in preservative

was prepared within only a few weeks of their

collection. Living specimens differed principally

in that the anterior and posterior surfaces of

the thighs were bright red and the skin of the

throat a deep yellow. The portion of the iris

above the pupil was pale brown and that below

it dark brown.

Comparison with other species: Litoria quadri-

lineata can be readily distinguished from all

other species currently known to occur in New

Guinea, but its phylogenetic relationships are

difficult to establish,

Ignoring the possession of the four dark

longitudinal stripes, which are not exhibited

by any previously described species, the size

and general proportions are consistent with

those exhibited by members of the Liroria

rubella complex, This group, as defined by

Tyler (1968), comprises L. congenita, L.

caputula, L. rubella and L. wisselensis. All are

of moderate size (snout to vent length rarely

exceeding 35 mm) and have short limbs. Dis-

tinct markings in these species, when present,

trend towards the lateral orientation so clearly

depicted by L. quadrilineata. Where L. quadri-

lineata differs from the members of the L.

rubella group most conspicuously is in’ the

nature of the digits in terms of length, pro-

portion of digits and webbing. In these respects

the only hylids with feet resembling those of

L. quadrilineata are the south-eastern Austra-

lian species L. brevipalmata and L. citropa,

74 M. J.

neither af which exhibit other obvious affinities

10 it,

In the key to. Papuan Jiyla (Tyler 1968)

(now CLitoriq, vide Tyler 1971). 2b. quedri-

lineata keys most closely to L. jendei, The

latter Species Jacks longitudinal markings, has

au higher TL'S-V ratio (0.48. us opposed to

0.39-0,44 in L. gradrilineata) and a consicer-

ably loner snout (E-N/IN [435 in Lh. fence:

and 1125-1182 in L. quecdrilineata).

Litovia quadrilineuia is a highly distinctive

New Guinea hylic frog, woe there is currently

no evidence of a paurticulariy close phylo-

venetic relationship with uny other species

known from the istahd,

Habitat: The series was collected on a plot of

low-lying, swampy vacant [and im the town-

ship, amongst matted grass above and adjacent

to waler. Collecting in similar habitats oceur-

ring to the east ane south-east of the township

vielled other speeies of Lireria, but no further

representatives of LF. auadrifineata were

observed or heard calling there.

Call: Most of the specimens were calling when

eallected. “Vhey were in a horizontal position

on the grass produvme u law-pitched huze-tike

call of approximately 2-3 seeands duration.

Phe species was by ne means timid, continuimy

to call whee illuminated by a spotlight.

Ranidella remota nsp.

Crinig sienifera, Roux C92),

Criniag stenifera xignifera, Parker (L940) tpartt

Holawpe: SAM R1AS24. A gravid female col-

lected ait Morehead, Papun New Guinea by

PF. Parker on 18 June, 1972,

Definition, Ao small lowland species (inales

13,2-15.6 mms: females 14.3-18.7 mm S-V)

characterised by its short and rather rounded

snout, lack of a tympentim, and smoeaih on

weakly granular abelominal ski.

Deserintion ol holerypes Maxillary teeth

present. Vomerine teeth absent. Snout short.

bhint and rounded when viewed from above

and in profile, and not projecting conspie-

vousty, Eye to naris distance slightly less than

the internarial span (E-N/TN 0.80), Canthus

rosiralis poorly defined ynd = straight. loreal

region slightly concave. Tympanim absent.

Fingers relatively long, unwebbed and un-

fringed. with well developed subarticular

tubercles. Hind limbs short (TLéS-V O44),

Toes Jong, unwebbed and with very slightly

developed literal fringes. A Small inner bul

no ouler pebatarsal tubercle,

TYLER & F, PARKER

Dorsal surtuce of head, body and limbs

covered with very small tubercles. Throat

smooth, abdemen very slightly granular, oA

glandular post-libial wren,

The dorsal surfaces of the body and timbs

dre dark grey with a pair of pale creamish

dorsal stripes extending from the scapular to

the cocevgeul regions. The ventral surlace is

pale creamy with a uniform, but yery sparse,

faint grey stippling,

Dimensions: Snout to vent length 16.5 mim;

bia length 7.3 mimi: bead length 7.2 mim; head

width 6.l mm: eye diameter 2.2 mm) eye to

nuris distance 1.2 mm: incernarigt span 1.5 nia.

Variation: There are 24 pyratypes consisting

of 6 adult females (3 of then gravid), 9

males (8 adult). and ®@ juvemles! MOCZ

S6119-21, SAM R1 3527-28, Crubam,

)O40,1972: UPNG 1190, Moreheud. 2h.7.19692

AMNH S$8O31—32, SAM R13525—26,

RI3681-82, UPNG 3847-30. MCZ 86127,

Morehead, 19...1969: MCZ 6122-26. NMB

44180, Merduke 1920; Morehead LS.vi.l 972;

MCZ SOTZR, Mata. vi i971. OF the pura-

types UPNG 1190 was collected by J. 1. Men-

vies, NMB 3180 by PL Wire and the remain-

der by F. Parker. A living specimen is depicted

in Pigure 3,

An additional & specimens (MCZ O11)

IS) were found in the slomach of it specimen

of the colubring snake 4eiplilesmig gird col

lected hy FP. at Morehead on p&.vi.1972.

These specimens ure identifiable as Ro remote,

hut ure so misshapen that ip has proved im-

possible to obtain measurements or uny other

Vata from them. Beenuse they have in ne wiry

gontribuied to our knowledge of the species

und have not been taken inte account in our

assessment of variution. we haye not accorded

them paratype stitus,

Snout to vent lengths of the adult mates

vary from 13.2-15.6 mm: gravid females vary

from 15.5-18.7 mm; the smallest juvenile 10.4

mm, Variation in proportions of tbe adults in

the paratype series are as follows: Th! S-V

0.44-0,50; HL HW 1.09-1,27; E-NVIN

0.80— 1.00,

Polymorphism in tents of dorsal skin’ tex

ture as defined by Parker (19400 and Main

(1957) involyes the smooth, lyrate and warty

morphs in the ratio of 8:52:10. Variation in

dorsy) appearance of most adults involves the

pair of longitudinal stripes extibited by the

holovyps, They vary only in their intensity and

extent of cantrast from the dull general dorsi!

colouritent,

NEW SPECIES OF NEW GUINEA FROGS 73

Fig. 3. Runidella remota.

Ventral markings are confined to very fine

und quite uniform stippling in all specimens,

except for one adult in which the throat and

pectoral regions are densely pigmented with

black, and bisected by ™ narrow, median un-

pigmented line.

In life the dorsum is either predominantly

grey or brown, the throat and ventral surfaces

of the limbs grey, and the abdomen white. The

portion of the iris above the pupil is gold and

the portion below grey,

Call: Males call from a horizontal position on

the ground, usually beneath a leaf or some

other form of cover, The animals appear ven-

triloquial, making it dificult to locate them.

particularly because they cease calling when

disturbed.

Data on the male mating call structure are

based on recordings made by J. L Menzies of

UPNG 1190 calling amongst flooded grass

tussocks by the river at Morehead on

28.1.1969,

A sonagram of this call is depicted in Figure

4, showing a dominant frequency of 4250 Hz.

a duration of 720 milliseconds, and being com-

posed of 14 pulses with an individual pulse

duration of approximately 28 milliseconds.

Menzies (pers. comm.) reports that there are

from 12 to 15 pulses per call and that the Jast

Iwo or three tend to have a shorter duration:

the ucoustic impression is one of a series of

short buzzes.

Comparison with ether species: The status of

the populations of Ranidella occurring in the

Northern Territory and in northern Queens-

land are currently unknown. Although it would

be preferable to have these populations defined

und described before describing what consti-

tutes the northern peripheral member of the

genus. we seek only to establish that the popu-

lution that we describe here is new, Thus,

although a close phylogenetic relationship may

ultimately be demonstrated with such northern

Australian species. we are now only uble to

distinguish R. remota from those species that

have been described.

Morphologically R. remora firstly must be

compared with the species known to occur in

Queensland: R. yignifera, R. parinsignifera,

und R. finnila. Absence of a tympanum and

the greatly reduced pigmentation of the ven-

tral surface distinguishes R. remota from each

of these species. Runidella tinnula is also

shown by Straughan & Main (1966) to have a

76 M. J. TYLER & F. PARKER

Oo +f O

L——— 1 second ——_

Fig. 4. Sonagram of mating call of Ranidella remata.

conspicuous snout, greatly projecting in pro-

tile, contrasting with the gently rounded snout

profile of R. remota.

Ranidella signifera extends from southern

Queensland to the southern portion of South

Australia. Many of the specimens from the

western portion of the range have reduced

ventral pigmentation, but the species is con-

sistently larger, Ranges of snout to vent length

for R. signifera derived from Littlejohn (1963)

and Littlejohn & Martin (1965) are: males

18.0-24.2 mm: females 19.0-27.7 mm.

Ranidella riparia of the Flinders Ranges in

South Australia is the only Australian species

known to lack wa tympanum. This species is

also consistently larger than R. remota with

snout to vent length ranges of 19,5-25.2

(males) and 23.0-25.2 (females). It also has

extensive ventral pigmentation and further

differs from R. remota in possessing broadly

fringed toes.

The most striking characteristics of the mat-

ing call of R. remota are its long duration of

720 msec and the number of pulses (14).

Within Ranidella this duration is considerably

greater than the ranges of all except one of the

species summarised by Littlejohn (1959) and

Littlejohn & Martin (1965). The upper limit of

R. riparia is quoted at 497 msec, but it is the

south-western Australian species R. glauerti,

with its maximum call duration of 820 msec

which surpasses R. remota. Ranidella glauerti

NEW SPECIES OF NEW GUINEA FROGS WV

differs in its pulse frequency (7-12). The

nature of the call differences between R-

remota and R, glauerti are not considerable, Of

the described Queensland species it is worth

noting that the call duration of R. tinnula is

Jess than 100 msec. The pulse rate of R.

remota is relatively low but such low rates

ure, in Ranidella, associated with a particularly

short duration in the species compared by

Liulgjohn (1959),

Habitat and habits; Tn the Morehead and

Weam areas, R. remota was found in areas

of low mixed suvannahs, particularly slong

the fringes ol low-lying gtass-covered flats

having a grey clay soil. The occurrence of the

‘species in low monsoon scrubland and_ tall

mixed savannas was restricted) to the area

around Balumok,

Ranidella remota was usually found away

from permanent water, and was observed to

be a secretive species living beneath leaf litter

and amonyst grass on damp soil, but was not

found beneath logs or bark fragments on the

ground. It appears to be predominantly noc-

turnal, although it has been observed hopping

amongst grass on days when the skics were

overcast,

Acknowledgments

We are indebted to Mr. J. I. Menzies

(University of Papua New Guinea) for per-

mission io reproduce the sonagram of R.

remota, to Dr. L. Forcatt (Naturhistorisches

Museum Basel) for the Joan of a specimen,

to Miss M. Anstis for preparation of the Jine

drawings and to Dr. J. Ling for reading the

manuscript,

References

BLake, A. J, D, (1973)—Taxonomy and rela-

tionships of myobatrachine frogs ( Lepto-

dactylidae): a numerical approach. Asi. J.

Zool, Zh, 119-149,

LitteevoHn, M. J. (1959).—Call differentiation

in a complex of seven species of Crinia

(Anura: Leptodactylidae). Evolution 13 (4)

452-468.

LirtLeJOHN, M. J. (1963).—Frogs of the Mel-

bourne area, Fic. Nat, 79 (10), 296-304.

Tiriveraun. M. J.. & Martin, A. A, (1965).—

A new species of Crinia (Anura: Leptodacty-

lidae) from South Australia. Capeia 1965

(3), 319-324.

Main. A. R. (1957).—Studies in Australian

Amphibia T. The genus Crizia in south-west

Western Australia and. some species from

guth-tastern Australian. Aust. J. Zool. 5, 30-

Moorn, J. A, (1954)—Geographic and genetic

isolution in Australian Amphibia, Amer. Nar.

88. 64-75.

PaRKER, H. W. (1940)—The Australasian frogs

of the family Leptodactylidae. Novit. Zool.

(42), 1-106.

Roux, J.. (1920).—Note snr Ja présence dti genre

Crinta, amphibien cystignathide, en Nou-

yee shinee: Rev. Suisse Zool, 28. (5), 118-

117.

SMRAVIGHAN, [. R. & Mam, A. R. (1966).—

Speciation snd polymorphism in the genus

Crinta Tschudi in Queensland. Proc. R. Soc.

Qlil TS (2), 11-28.

TyLer, M. J. (1968).—Papuan hylid frogs of the

genus Hyla. Zool, Verh. (96). 1-203.

Tyver, M. Jj. (1972a).—An analysis of the lower

vertebrate faunal relationships of Australia

and New Guinea. Jn D. Walker (Kd.)

“Bridge and Barrier: the Natural and Cul-

tural History of Torres Strait.” (Dept, Bio-

gcography and Geomorphology, Publ. BG/3

Australian National University, Canberra, )

TyLer, M. J. (1972b).—A new genus tor the

Australian Jeptodactylid frog Crinia darline-

toni, Zool. Meded., Leiden 47, 193-201,

Trier, M. J., & Menzies, J, 1. (1971). -A new

specics of microhylid frog of the genus

Sphenophyrne fram Milne Bay, Papua. Trans.

R, Sac, S. Aust, 95 (2), 79-83,

Tyter, M. J. & Parker, F. (1972),—Additions

io the hylid frog fauna of New Guinea, with

description of a new species, Literia timida.

Trans, RK, Soe, 3. Aust. 96 (3), 157-163.

vaw KAMPEN, P. WN, (1923),—The Amphibia of

the Indo-Australian Archipelago, (Brill:

Leiden, )

EARTHWORMS (OLIGOCHAETA: MEGASCOLECIDAE) FROM

SOUTH AUSTRALIA

BY B. G. M. JAMIESON*

Summary

JAMIESON. B. G. M. (1974).-Earthworms (Oligochaeta: Megascolecidae) from South Australia.

Trans. R. . Soc. S. Aust. 98(2), 79-112, 31 May, 1974.

The Megascolecidae is the only family of earthworms indigenous in South Australia.

The megascolecid fauna of the state is impoverished, though specific endemicity is high, consisting

of five genera with thirteen species. These are the circum-mundane Microscolex dubius (Fletcher,

1888a); the new endemic species Perionychella (P.) inconstans, Spenceriella imparicystis,

5. penolaensis, Gemascolex bursatus, G. mirabilis, G. octothecatus, G. similis, and G. walkeri spp.

nov.; the previously known endemic species G. newmani Edmonds & Jamieson, 1973, and

G. stirlingi (Fletcher, 1888a); and two species known also from Victoria, G. lateralis (Spencer,

1892; syn. Megascolex zeitzi Michaelsen, 1907b) and Heteroporodrilus shephardi (Spencer, 1900).

the latter being represented by the new subspecies H. shephardi armatus. In sharing its four

indigenous genera and two of its species with Victoria, South Australia shows close zoogeographic

affinities with this state whereas affinities with Western Australia are minimal, consisting only of a

close relationship between Perionychella and the Western Australian genus Graliophilus.

The paucity of the fauna is attributed to the low rainfall and it is noted that ten of South Australia's

thirteen species have excretory adaptations, in the form of intestinal enteronephry, which favour

water conservation.

EARTHWORMS (OLIGOCHAETA: MEGASCOLECIDAE)

FROM SOUTH AUSTRALIA

by B. G, M, JAmMrEson*

Sunimary

Jamitson, B. G. M. (1974).—Rarthworms (Oligochacta: Megascolecidac) trom South Aus-

tralia, Vrans, Re Soe. S. Aust, 9 (2), 79-112, 31 May, 1974.

The Megascolccidae is the only family of earthworms indigenous in South Australia,

The megascalecid fauna of the state is impoverished, though specifle endemicity is higl, con-

sisting Of five genera with thirteen species. These are the circum-mundane Micrescolex dubins

(Fletcher, (8884); the new endemic spécies Perionychella (P.) incenstuns, Spenceriella impari-

crysis, S. penolaensis, Gemascolex bursatus, G. mirabilis, G. octothecatus, G. similiv, and G.

walkert spp. nov.; the previously known endemic species G. newniani Edmonds & Tamieson,

1973, and G, sitrlingi (Fletcher. 1888a); and two speci¢és known also from Victoria, G.

lateralis (Spencer, 1892; syn. Megascolex zeifzi Michaelsen, 1907b) and Hezeraperodrilus

shephardi (Spencer, 1900). the latter being represented by the new subspecies H. shephareli

armatus. In sharmg its four indigenous genera and two of its species with Victoria, South

Australia shows close zoogeographic affinitic¢s with this state whereas affinities with Western

Australia are minimal, consisting only of a close relationship between Periarychella and the

Western Australian genus Graliophilus. The paucity of the fauna is attributed to the Jow

rainfall and it is noted that tea of South Australia’s thirteen species have excretory adapta-

tions, in the form of intestinal énteronephry, which favour water conservation.

Introduction

Three indigenous species of earthworms

(Family Mepascolecidae) have previously been

recorded from South Australia. All were

assigned to a single genus, Gemascolex by Ed-

monds & Jamieson (1973), The three species

are G strlingi (Fletcher, 18882) of which

Megascolex flercheri Shannon (1920) is a

junior synonym; G, zietz? (Michaelsen 19076)

which (see below) is a junior synonym of G,

lateralis, (Spencer, 1892); and G. sewmani

Edmonds & Jamieson, the type-species of

Gemaycolex, The only other megascolecid

carthworm previously recorded from the state

is Microseelex duhius (Pletcher, 1888), for

which Adelaide is a type-locality, This species

is curyhuling and is circiim-tnuodane jo

warmer, though not tropical, regions. Its cen-

tre of origin is unknown.

‘The only other earthworms from South Aus-

tralia belong to the holarctic Family Lumbri-

cidae. This non-indigenous family is beyond

the scope of this work. It is nevertheless of

interest to note jocalities from whigh lumbri-

cids were obtained in the present survey and

these are included in the map (Fig. 1).

With the assistance of Mr. T. Walker, the

author collected earthworms in August 1972,

after favourable rains, from 26. localities (see

Fig. 1), from Mt, Remarkable in the north

to the Fleurieu Peninsula in the south. Collcct-

ing yielded twelve species of Megascolecidae,

including the three previously described

Gemascolex spp. and Microscoler dubius. A

further species, collected by Mr. Ifor Thomas

from Kangaroo Island, brings the total of

known megascolecid species from the atate to

13. No collection was done on Yorke and

Eyre Peninsulas in the west. nor in much of

the wetter south-eastern portion of the state,

and it seems likely that further species will be

found in those areas. It is hoped that this

study will stimulate others to make the further

collections necessary to yield u definitive check-

list of South Australian earthworms,

Systematics

The megascolecid species of South Australia

fall into the subfamilies Acanthoctrilinae, rep.

> Zoulogy Depariment, University of Queensland, S1. Lucia, Of¢ 4067,

Fig.

B. G. M. JAMIESON

H | J K L

bet tl

34°

35"

ta) fe} o

ig 138° 139° 140 141

Map showing all known records of earthworms from South Australia. White circle, Megasco-

lecidae only. Black and white circle, Megascolecidac and Lumbricidae. Black circle, Lumbrici-

dae only.

EARTHWORMS FROM SOUTH AUSTRATIA a4

reseed by the tribe Acanthodritini, and

Megascolecinae, represented hy the tribes

Pertonychini and Megascolecini sensi Jamie-

son, 19714. The sub-families and tribes are set

oul in this order in the present account and

the species are listed in alphabetical order

under their genera within. each tribe, Abbrevia-

tions fer institutions in which specimens have

been lodged arc; AM (Australian Museum, Syd-

ney), BJ (Author's collections), BM (British

Museum (Natural History)) and SAM {South

Australian Museum). ‘Vhe major collectors,

B. G. M, Jamieson and T. Walker, are indi-

cated by the initials HJ. anc 7.4’, respectively,

The abbreviation H signifies holotype and P

paratype. Explanations of terminology used

in descriptions may be found in Michaelsen

(1900). Stephenson (1930) and (nephridia) in

Jamieson (1971a).

A key to the Megascolecidae of South Aus-

tralia follows. To permit ready identification,

without necessitating detailed study of the

excretory systeny which is the basis for tribal

elassificalion, tribes have been omitted and the

key proceeds directly to species. As unknown

species muy be cncountered by collectors,

agreement with illustrations cited in the key is

required, and the detailed descriptions should

be checked to confirm identification.

Family MEGASCOLECIDAE

Subfamily ACANTHODRILINAEF $s, Jamic-

son, 197La

Tribe ACANTHODRITINI s, Jamieson, 1971a

Holonephric, or, if wholly or partly mero-

nephric, with a single pair of prostates. Pros-

tates tubular, one to three pairs. Stomate.

meronephnidia, where present, not forming a

series median io astomate micromeronephnidia,

Genus MICROSCOLEX Rosa, 1887

Microscolex dubins (Fletcher. 1888), Rosa,

1890; 511. Michaelsen, 19079: 146-148;

1907b; 5. Pickford, 1937; 429-432, figs

398-399_ Gates, 1962; 7-15.

FIGS 2A, 12; TABLE 1

Eudrilus (?) dubius Fletcher, t®88a: 39$=381,

Length = 36 mm, Ww (midelitellary = 3.4

mm, s — 88 (specimen 1), Circular in cross

seclion. Pigmentless in alcohol, Prastamium

not canaliculyte, cpilobous 1/2, closed. Peris-

tomium not bisected ventrally, Dorsal pores

ubsent. Setac & per segment, commencing int

HI, in regular longitudinal rows throughout.

Setae a and # absent in XVII.

Key to the megascolecid species of South Australia

|, Combined mule and prostalic pores a pair an XVIU (16th setigerous segment), Spermithecul

pores. absent

Mierase alex dubs, Fig. 2A

1. Combined male and prostatic pies a aa ‘on XVID Vath setigerous segment). ‘Spermuthecal

pores present. _

2, Nephtidia one pair per segment

2. Nephridia several to many ino segment

Nephridia with terminal bladders which alrernate from. Jateral to ventral . Ho dstihetinsa seit

Heteroporadrilus shephardi. armiatus, Fi ig- 2B

3. Nephridia without bladders; ducty in w sinete series on each side

Perienychella (P.) inconstens, Fig. 6c

4, Caloiferons glands present of the oesophagus, paired in X, XT-XTIT ‘terre etiasettos 5

4. Culciferous glands absent

5 Calelferais elands 4 pairs, in X-XI1. Spermathecus Mrpdined “Spenseriella Intakes vavix, Fig.

5. Calciferous glands 3 pairs, in XTX, Spermathecae paued ..

6, Spermathecal pores J pair, in 5/6.

6. Spermathecal poren more thin J pair, ip 7/8 ot 8/9 anteriorly vectra

7. Spermathecal pores 2 paire |... .,

7, Sperinathecal pores more than 2 pairs

8. Last spermathecal pores in 7/8 ...

8. Last spermathecal pores. in 8/9

9. Spermathecal pores 4 pairs paiavesiacs Dito

9. Spermathecal pores 3 pals...

10, Lust hearts in XI.

tO, Last hearts in XILT

. Genital marking(s) unpaired, midveotral .

. Genital markings paired on

—_"

——

a 6

.. Spenceriella penolaensis, Fig. 9B

Gemascolex walkeri, Fig.

Gemaseolex jiirabilis, Fig. 5

oor ort Gemuxcalex Pursatus, Fig. 3A

Gemascolex octothecains, Fig, 6A, B

Gemascolex lateralis, Fig. 4A. B

Gemascolex newrrani. Fig. 7B

12. Male pores whout one third of the body circumference apart. No ‘genital markings present

behind them

Gemascolex similis, Fig. 3B

12. Male pores about one fifth “nf the © body. eiremifereaice apart, Paired genital markines be-

hind them

(tas ase cnt Gemascolex stirling’, Fig. BA, B

o2 B. G. M, JAMIESON

TABLE i

foerseral elistancey in Mierascate, dubius

Ct a ) |) |

Seement Nal he te 11 TY 62 io 2 (U6

Segment XM rb GS th bl Fs 19 17 OF

MAnddrdiyed as Up of clicumfereme

: au sb be ed dd de cb ba

Svement KET G90 65 4G 10S 248 116 4d GR

Senment XX i500 3.1 15,3 11.7 277 10.2 178 fh

Mean 107 6.0 13, 112 1635 103 150 60

Literval/alhy 1A if Ls 19) 4:1 1 27 10

Nephrepores inconspicuous. in the interseg-

mental furrows 9 little less than 1/3 be below

e first observed at 6/7. Clitellum annular,

XIL-XVI with weak development through

AVIL well developed but not strongly pro-

uiberuni, apparent ay a smnoth region owing

IO suipression of Intersevmental furrows. 14/15

and 15/16; setwe and nephropores retained.

Male pores minule, equatorial in XVIT, lateral

of seta) lines a, euch in un oval field, which

is not stiliciently elevated to be termed a poro-

phore, the pores 1.26 mm, 0.14 circumference,

apart. Accessory genital markings absent. Fe-

male pores paired, almost ul the anterior mar

gin of XIV, shorily median of «lines.

Spermathecal pores absent.

Strongest septu 8/9-13/ 14. moderately

strong, Dorsal blood vessel single, continuous

onto the pharynx. Last hearts in XI, those in

X-XIT latero-ocsophageal, tach with a con-

neclive From the dorsal and [rom the poorly

distinguishable supra-ocsophageal vessel; the

Jatter oesophageal only, Commissuraly in VI-

{X dorsoventral only, Subneural vessel absent

Gizzard rudimentary, in V. Ocsophsgus thicker

walled! and more rugose internally in X-X1V

than anteriorly, monlifarm throughout though

narrower in XV. Extramural culciferous glands

absent. Intestinal origin XVIL; cyphlosole. caeca

and muscular thickening absent. Nephridta

stomate. vesiculate helonephridias those in T-

IV each sending a duct laterally to discharue

presetally in d@ line, the duct in TI avesicu-

late, the duets ia TIF and TV each with a smull

subspherical bladder; the nephridia in V dis-

charging through emall subspherical somewhat

crenulated bladders preserally immediately

pelow c lines, the bladders joincd medtunly

and slightly suhterminally by the ducts; by

seement VIIY the duct median to the bladder

is itself swollen ond by XI the original bladder

protrudes from. the lateral aspect of the wedge

shaped expansion of the duct and may he con-

sidered a short rounded diverticulum; the

bladders reach their furthest separation from

¢ line, at approximately one fourth ch. in the

vicinity of XVIL und maintain this postion

further posteriorly. Caudally the diverticulum

becomes 2 definite lateral caecum, about twice

as long as wide, though hidden by coils of the

nephbridium. Holandric, clavate testes and) non-

iridescent funnels in & and Xf; seminal vesicles

2 pairs, racemose, in XL and XL. Metagynoas;

ovaries, flattened johes with severy) conjoined

strings of large oocytes, aad ftunfels if XTTT;

small ovisacs in XIV. Prostules almost

Straivht, tubular, passing laterally From the

ducts in X¥YI1 and widening evenly to the

rounded free extremity so as to appear slen-

derly clavate: the external duct indistinctly

demazcated but with a shizht musculur sheen

the double vas defetens joining the duct at its

ental third. Penial setae present in two follicles.

tt and &, the & follicle entering the body wall

in common with the prostate duct. Buch peri-

setal follicle with two functional and two

reserve selue: each scta almost stevight, ectally

tapering slightly to a blunt point. the ectal

fifth bearing a longitudinal series of approxi-

mately 7 to 10 circumferential sets of shart

transverse incisions: the posteriur border of

each incision forming a few minute anteriorly

directed denticles, the incisions in a set

arranged obliquely vround the circumference

of the seta; this ornumentation poorly visible

under the light microscope: Jengths of two

functional setae 0.52 und 0.72 mm, general

width of the shaft 16am and 26ym Tespec-

tively. Spermathecae absent.

Marertal examined: Lm). 140°S5'E, 38°01'S,

26 km from Mot. Gambier along road to

Nelson. in sandy loam under sriss among

wattles and gums and same garden escapes.

Ba. aad TA, Wii 1972— 2 specimens

(BJ).

Type-lacality; Sydney, Mulwala (N.S.W,):

Adelaide.

Other Australian lacalities; Tas, (hide

Michaelsen 1900); N.S.W—Neweastle. Para-

matta (Michaclsen 1907a, b)> lenolan Caves

area (Boardmin 1943}, South westem Ans-

tralid | Michaclsen 190747, Old ‘Toowoomba

{Stephenson 1933). AC.T., (Gates 1962),

Remurks: Microscalex dubias is a euryhalioe

species circum-mundane in the northern und

southern hemispheres mostly in warmer

regions, though not tropical,

Absence of spermathecal pores, location of

combined mule and prostatic pores on XV

and progressive narrowing of setal interval a

in an anierior direction from approximately

EARTHWORMS FROM SOUTH AUSTRALIA 83

Fig. 2.

armatis, holotype. 111.

Genital fields of: A, Microscoiex duhius, specimen 1, Lml. #, Heteroporodrilus shephardi

Symbols used in illustrations of genital fields: 9, female pore; g.m., accessory genital marking: ¢,

male pore; sp.p., spermathecal pore, Roman numerals are segment numbers, Clitellum shaded, All by

camera lucida.

segment XXIL to XVHI allow ready recog-

nition of this species.

Subfamily MEGASCOLECINAE s. Jamieson,

19712

Tribe PERIONYCHINI 5. Jamieson, 19714

Male and prostatic pores coincident or

(Diplotrema part, New Caledonia) near

together on XVIII; sometimes with a single

median combined mule and prostatic pore.

Prostates one pair, tubular to racemose,

Purely holonephric, or with meronephridia in

a varying number of segments anterior to holo-

nephridia; never (7?) with intestinal entero-

nephry.

Genus PERIONYCHEBLLA Michaelsen,

1907a

Perionychella (P.) inconstans sp. nov.

FIGS 6C, 10A; TABLE 2

4 R, G. M: JAMIESON

Length = 63(H)-77(P1) min, Ww (mid-

witellur) - 2 mm, s — 122(H)=-131(Pt).

Pigmentiess in alcohal with the exception of

the teddish brown c¢litellum, Form attenuated;

circulur in cross section. Prostomium epi-

lobous 2/3, acute. closed: not canaliculute,

Peristamium not bisected ventrally. Setae 8 per

segment, in regular longitudinal rows through-

out (H) or cand ¢ irregular posteriorly (P1};

a and 4 absent in XVII.

Nephropores sporadically visible, on and be-

hind the clitellum, anteriorly in their segments

in & Jines, Clitellum annular, very conspic-

ueLs Owing lo streng lumescence and its red-

dish color (almost fusiform and reminiscent

of thal of the aquatic eenus Sparganophilus),

clearly demorcuted in XIL-2/3 XVIII, but

some clitellar modification and pinkisly pliamen-

lation present throughout XII and XVIII dor-

sally, ne. extent XII-XVITT (= 7 seements);

intersegments 13/14-17/1L8 totally obliterated

dorsally. Male purcs equatorial in a lines of

AVILL on strongly protuberant, subcircular

papillae which fill all buc a small anterior part

of the segment, the lateral borders of the

papillae less clearly demarcated than the

median borders, The papillae tie in a whitish

glandular field which interrupts the clitellum

from shortly presecally in XVII, Isteratly be-

yond & in XVEL and XWITT, and which extends

posteriorly to include (H) or just preeede {P1)

the sctal are of XX. The sete! annulus of XVII

to shortly lateral of / forms a transverse ven-

tral Hidge Mistinct yecessory genital markings

are not recognizable in the male field but

there § a suggestion of a Lransverse pucl trom

mid wh to Interal ef f on each side filling the

anterior third of XVILI An unpaired, midven-

tril, citoular accessory genital marking with

depressed central area and porelike centre

almost fills the length of each of segments

VT. VO and TX and extends Jaterally ta «

Gr into ah (HR, Pl; seé Field Variation)

Female pores paired. shortly antenor to (H)

er anteromedian (PL) to setae a of NIV. in a

common glandulsr field which fills 45 and

longitudinally extends from 13/14 posteriorly

to just include the ventral setal couples.

Spermathecal pores in 7/8 and 8/%, ench on

an inconspicuous papilla almost concealed in

the intersegment, unpaired midventral (P1) oF

paired immediately median to a lines (H).

Thickest sepla 7/8-9/10, moderately

stronety thickened (H, Pl). Dorsal blood ves-

sul single, continuous onto the pharynx (HH).

Last hearts In XIE, those ty K-XIT Jatero-

TABLE 2

Hitersetal distunces im Perionychella (P.) incanstans

aaoab Oh Uc te ich

Setment XA

Holotype oS O82 OF O48 Fa 4 Of FF

Patiwere 1 U3 02 vs 03 2 us O04 Ut

Sevment XX

Tiolotype “4 02 O4 45 20 %O8 O45 BE

Paratyne | Oo O02 US 03 20 O03 D4 92

Slnidardized oy %0 Gt crrcumference

aaa ced dd de och by

Seament X11 . * .

Holotype 06 41 le 74 466 OS 48 oO

Paratype J 77 Sh OT t> 49nN 7,7 SB AS

Mean 91 AT WR HT ak? 7 os 49

Totervale at a Fh Bs 14 102 5 21 io

Sevinent NK

Holotype OF do if FS 264 GF INT ae

Patatyre Sy SY [Ue 64 472 59 BO 50

Muar Qn 49 112 BI ARR 4A OH Ad

Imeryalan 2 1 243 20 4S Pe een ee

oesophageal, each feceiving a connective from

the dorsal vessel and from the aupra-oesopha-

geal vessel. The Jatter vessel extends Fram 1/2

VUL XIV (Pl), 1/2 XV (HI) and except

al its extremities, is larger than Uhe aborsal

vessel. No subneural vessel detectable.

Gizzard smal) and glohose in V, its posterior

limit being at 1/2 VI, muscular byt easily

compressed. Oesophagus monilitenn bul mo!

evidently vascularized in VI-VI1, in EX-XLV

moniliform and apparently with tnereused

vascularization (especially vascular in IX1, in

XV-XVIT (H)-XIN (PH) tubolic and ante

slightly vascularized, in NVHL 1H) similar to

that in XVIL hut sinbose, Intestinal origin

apparently XIX where the wall is thinner (BH)

or XX (PI, with oesophageal valve at 19°20).

not reaching full width until XXT: tvphlosole

absent, though # rudimentary mid-dorsal ridge

is observable in paratype J. muscular thicken-

ing and cacea absent fH, Pl}. Nepbhrisia

holanephridia first recognizable jn XI (PL) or

XIE (1H) hit 2 pairs of small tuitlike struce

tures on the badly wall, in TV and Vo ¢P1) may

he tufted nephridia (the extreme nuarmowress

of the worm tendering dissection very diffi-

cult); each holonephridium with a lute pre-

septal fudnel and narrow «uct discharging

presetally in A line,

Holandric. testes and iridescent funnels [n

X and Ny seminal vesicles lure, racemose,

with many large discrete Joculi, in IX and XI,

Melugynaus (ovaries consisiing of ai few

irregular chains of very large oocytes and fun-

nels in XPM) true ovisics, each with) several

very large oocytes, in XIV. Prostates a palr

of thick short tortuous tubes restricled to

XVII €PL) or their ental ends just entering

XIX (11); muscular ducts straight ov slightly

curved, not sinnous. Penial setae present, their

EARTHWORMS PROM SOUTH AUSTRATIA 35

follicles extending from XVIII into XX, fill-

form.

Spermathecae in VILL and 1X, each with a

succiform, narrow-slalked ampulla anu uw digiti-

lorm-clavate (inseminaled) sinuous diverti-

culum joining the base of the duct and longer

than duct plus ampulla, In paratype 1 there

is Only a single spermatheca in each segment,

its duct entering the body wall helow the ven-

tral nerve cord. In the holotype there are 2

spermathecue in cach segment, discharging

median to « tines, and the right spermathecu in

each segment has a replicated ampulla,

Field variations The male genital ficld has the

form described for the holotype in the 9 speci-

mens selected as paratypes but the right pros«

fate (and male porophere) is replicated in

paratype 4 so thot there is one in X'VIIT and

a further one in XIX, Midveniral unpaired

accessory genital markings are present in VIT,

VUL and EX in 3 specimens fineluding the

holotype), in VIT and VII, in 3 specimens, and

in VIL and &X in 4 specimens, Spermathecal

pores, in 7/8 and 8/9, are paited shortly

median of 4 lines in 3 specimens, paired but

ventrally almost contiguous in | specimen, and

are unpaired, midventral. in 3 specimens, being

externally unrecognizable in the remaining

specimen,

Material examined: Hjl, 136°44'E, 35°56'S,

in soft. waterlogged earth, bonded with grass

and grass Toots, on the banks of Rocky

River, about 1.6 kim N of Rocky River

Homestead, Kangaroo L.: approximately 50

worms per square foal, f, Thomas, date?—-H,

PI-9 (plus many additional specimens), H,

P2+ (AM): PL. 5, 6(BM); P7 (SAM): BS,

8 and additional specimens (BI)-

Remarks: This species differs fram others in

Perjonychella in location of nephropores in &

lines and In that cd is not as large relative to

eb. These differences may indicate that it is

phylogenetically Wislinct from the remainder

of the genus but erection of jy separate genus

for its Teception does not appear necessary.

Genus HETEROPOGRODRILUS Iamieson.

1970

Heteroporodrilus shephardi (Spencer.

armatus subsp, nov,

FIGS 2B, 18, 1fA, 13; TABLE 3

Length = 113+) mm-132¢P1) mm. w

(midelitellar) = 76PE)-BYH) mm. s = 109+

CH, pesterior amputee: Pl damaged), Form

angular in cross section the periphery being

1900)

straight between adjacent setal lines Pigmented

ereytsh brown but pale yentrally in alcohof,

Prosionium protanylobous, with a transverse

furrow at O/1 (H) of epitanylobous with a

transverse Durrow at + Ll; the peristomium with

several longitudinal furrows so that extension

of a dorsal prostamial tongue to 1/2 is ques-

tionable. Canalicula absent, First dorsal pore

6/7 (H, P1), Setae & per segment, in regular

Inngitudinal sows throughout; setae a and #

absent, replaced by penial setae, in XVIIL

Nephropores conspicuous, anterior in ¢heir

segments in the holotype in I(7), HI-IV ig

d lines, in V~TX alternating from d@ to mid he

(commencing in V in d on the right and mid

he on the left); thereafter alternating from

d to 4 (in X in } on the right and ¢ on the

left); the nephropores symmetrically disposed

in paratype 1: in II-T¥ ia d lines; in V and VI

in mid Se; in VIT-TX alternating from d@ co mid

be; in X backwards alternating from > to

d {examined 1 H und Pl to 20/21). Clitel-

lum annular, XIV-J/3 XVI; dorsal pares

occluded in 14/15-16/17; intersepmental fur-

rows fainter dorsally; setie and nephropores

elearly visible. Mule pores on XYVIIL ih }, each

on a slender pupilla strongly protuherant fram

=n indistinct Jow circular prominence. Aecces-

sory genital markings: transverse oval to ob-

long pads with porelike centres in VI (imi-

lateral, right), VIL and VIIT (paired) filling wh

and with centres at or slightly behind the setal

are; similar but larger pads almost filling the

segments longitudinally and with centres

immediately presctal in wh paired in XT und

XH and unilateral, right. in MXIT: paired deep

pits in wh in 197/18 and immediately behind

TABLE 3

feterseral distances in Hetevaporodrilis shephardi

Armatos

ie ab fe 4d dd fe ch bs

Seorrent XEL

Hoalatyne 76 21 53 TR GAR AG at 1

Paratvee 2 23 |.d 222 24 d4 24 22 19

Paratype 4 19 LS 2A 26 54 2H 2.2 15

Sverrent NX

Holatyor 30 16 25 aS £2 49 29 IS

Vurarypu 2 743 12 18 29 44 38 22 4

Poravoe 3 19 J3 24 234 42 24 24 11

sruncdurdined as % of ciredinference

oooh he ed fh de och ba

Seyment N11

Holotype 9h 7.5 192140959 15 1.4 7.0

Purecype 2 21 74 116 12.6234 126 11.6 9.0

Paratsne $ 9S FA UG IL AT WA WY 7S

Mean Wa THUS 1228.1 2B 4 TR

Tnietval/ah 14°10 16 58 948 7.7 15 10

Seament XX

Holatype 117 62 135 189 MA 14. LL 8

Purarypo 2 4,9 G2 8:2 15.0 DB 40 The TI

Taraiype 3 92 F8 126 126 IZI2SIZS 58

Mean W.5 G4 11,1 14.3 24.7 143 118 84

Tnterval/aly 17 1.0 1.7 22 59 22 18 1.06

eG 8B, G M, TAMTBSON

Te 19, a small indistinct eyelike marking

present postero-luteraliv to cach pit (H, se¢

Ficld Variation), Female pores inconspicuous

midway berween the setal arc and anterior

horder of NIV, shortly median of a (H. PI).

Spermuthecal pores 3 pairs in 6/7, 7/8 and

8/9, in b lines land with inconspicuous ellip-

tical lips, (EE)} or shortly Lateral of & lines.

and preceded by 4 semicirculor swelling which

fills the postenor third of the previous segment

(FL).

Septa 8!9-11/12 strongly thickened. Dorsal

blood vessel single, continuous ou the

pharynx. Supra-cesophageal vessel traced into

VII, nat demonstrable in VIL, ending pas-

teriacly in XTIL, receiving a transverse vessel

from each of the calciferous lands, in X—XU-

List beurts i OKIE, those in X-XUL, which

are stont, originaling from the calcilerous ves-

sels and receiving slender connectives Trom

the dorsal vessel flatero-oesophageal hearts);

coummissurals ta VIT-IX more slender, dorso-

veotral only und, unlike the Iqltero-Gesuphugesl

heurts, with parietal branches but mverthe-

less valvular; vessels Trom the dorsal vessel in

Vo wid VE beanehing on the gut. Gizzard broad,

wossy. slrang hut fhitly easily compresnible

(tt) or elongate and firm (P1), the preeeding

oesophagus, in TY, forming a wide Maceit pro-

yebtriculus. QOesophagis unmedified in 1X,

bearing 4 pairs of ventroluteral browdly sessile

extramural culcifecous glands, in N—-XII, the

lumen of each gland jlmost occluded by

Aumerous Tadial lamellac. Oesophagus short,

narrow and chlorayzogendouy sm XTV, Latestinal

origin’ XV. typhlosole absent. Wolonephric,

nephridia with moderately lurge subspherical

lerminal yesicles, Which are readily visihle in

the posterior intestinal region, are lnss well

developed in the anterier intestinal region und

not apparent in the forebudy; preseptal funnels

large. i ah irrespective of position of bladder

(first demonstrated in XIV), Compacted

sperm masses surrounding iridescent sperm

funnels in X sind Xl, seminal vesicles tace-

mose, i) TX and XI, Laree racemus¢e prostates

a pair. in XVI XXE. 9 U-shaped muscular duce

passing medianly from the middle region of

the gland; the dice bifurcaiing at its ental

exitemity 1® receive ducts from the pntetior

and posterior portions of the gland) vas

leferens joining the duct near its ectal end,

Penial setae slender, sittuous, almost filiform,

the ectal region, viewed from either side. ornu-

mented with irregular, approximately trans-

verse to oblique rows of a few (P71) Io several

(H)} triangular llavlened scales, which except

at their bases, are free fram the setal surface

but point towaruls the ectal extremily ol the

setay the scales in the hulotype with single,

bifid ur trifid points and in two or three groups,

each group corresponding approxinyaccly with

one of the courser scales of paralype 7; total

number of scales counted in u fongitudinal

line approsimutely 20 lin 0.21 mm) anil 37

fio 0.44 mm) in two sete of the holotype;

eqch scta tapering to a rounded bul delicate

point: length of a fully developed seta

2.9(P1}-3.71H) mm; width of the most

strongly ornamented region 27 or 20 pm (H)

gnd 23 yam (PI). Female organs no ohserv-

able (EH); ovaries with numerous egg strings,

ynd funnels ia XIE; ovisucs absent. Spermathe-

exe three pairs discharging antenorly in thetr

teements; umpulla subspherical, slightly shorter

than the stoutly fusiform muscular glossy dacr;

an abruptly widening clavate diverticulum less

than one third the Jength of the duct arising

from the median aspect of the duct shortly

etal of the ampulla (H. PI)-

Field variajon: Th the four type specimens

paired pads in @b, which Jo not include the

anterior portions of their segmenis, are

present in VI. VIL and Vill in H (R), P2 und

P3, A liplike swelling extending to the preced-

ing setal arc is present in these segments in

front of each spermathecal pore in PI—3, An

unpaired midventral circular posisetal marking

with porelike centre is present in cach of sex-

ments VI. VJ1 and VIE in P2 of in VUIE only

in P3. Paired pads median to setac 6 anc occu-

pying much of the length of the segment are

present in Xin PT ahd P3. in Xi in H and Pl

and 3, and in NIL in Hy, P2 and P3. Paired

pits in ab lie in intersegment 17/18 sud im-

mediately behind 18/19 in H. Pl, 2 and 3.

Puired oval pads in wd occur in XXUL in P2 hut

there is only one. unilalleral pad i) HER),

PCR) and P3(L1. Indefinite turmd areas miry

be present in the vicinity cf the paired pits of

(7/18 and 18/19, Le. ill defined eyelike mark-

ings postervlateral to the pits in XVUL and

XIX in H or posteromedian ta the pily in

XVII in Pl and P3 and tn XEX also in PL.

Material examined: LIN, 140°49'F, 37°28’,

1) km S of Penola in eucalypts fringing

Pinus radiata. BJ. and TW , 15,viii-1972-H.

Lk2, 140°42°E, 36°37°S. 37 km from Ror-

dertown along road to Naracaurtr, In bank

of temporary pool in grassland with sparse

yrassirees aad cucalypts, T.-H, L6,vili,1972—

P4, 1k4, L40°44VB, 36°59'5. 2 km & of

EARTHWORMS FROM SOUTH AUSEPRALIA ny

Naracoorte, jn sandy soil With bracken and

watten fear pasture, By, and TLiW.,

fo.viin.1972-Pi-3. HtAM}; PI-2(B));

P4( BM): P3(SAM}),

Remarks: The new niaterial werees with H,

srepharai alone in the genus (vide Jamieson

1970) tn alternation of pnephropores between

@ and mid be, rather than the usual d to e,

and it is here included in AY shephardi as a new

subspecies although it shows ditferences. in-

eluding the distribution of genital markings

und the presence of penial setae, which might

be considered to warrant separate specific

status. Whether or not it be reproductively

isolated from: the numinute subspecies it is

unquestionably, from its morphology, more

closely related to the latter than to any ether

taxon in Heteroperodrilus. H. shephardi be-

longs 19 a group of species with four pairs of

ealedferous glunds, the other members of which

are AH. eanatleularus (Fletcher }889a) and HM.

muyiterreus (Pletcher 1888h). The latter two

Species Occur lerrestrially in upper reaches uf

the Murray-Darling river system while /f,

shepard occurs on the Wimmera River,

Tribe MiGascoLeomr s. Jamieson. 197 1a

Male and prostatic pores coincident on

XVI (rarely XVII); prosiales one pair,

racemose (wilh branched internal ducts and no

Single central lumen) or tubular (with a single

centeg! lumen). Purely meronephric; median

stomate néphridium, if present, opening into

the intestine,

Genus GEMASCOLEX Edmonds & Jamieson,

1973

Terresira!. Body circular in cross section

or (G_ dursetes) dorsoventrally depressed.

Frostumitim epilabous to tanylahous: peris-

tomium bisected by 9 longitudinal furrow ven-

Lrally, which is more conspicuous thon other

srmooving which thay be present, or (G. shira-

bility and G. stirling?) grooving present all

round but not more conspicuous venérally.

Setae numerous (more than 8) in each seg-

ment, Nephropores not externally recognizable.

A pair of combined male and prostatic pores

on XVITL Clitellum annulat anterior to 18/

19: its intersegments and dorsal pores obscures

at maturity but setae visible. Intersegmental

accessory genital markings alwavs present. Fe~

male pore presctal in XIV and midventral or.

as # rare individual variation (G_ lateralis),

paired, Spermathecal pores 24 pairs in $/6-

8/9, 3 pairs in 6/7 and 7/S, or a pair in 5/6

only.

Dorsal blood vessel single; continuous onto

pharynx. Hearts in X posteriorly latero-

ocsophageal. each arising trom the shart supra-

oesophageal vessel and from the dorsal vessel,

Last hearts in XII er XII, latero-ogsophageal

vessels (always?) present median to the hearts.

Subneural vessel absent. Gizzard large, in V or

VI. Oesophagus lacking extramural calciferous

glands, Intestine commencing in XVII; a ridge-

like low or (G. walkeri) deep dorsal typhlo-

sole present; caeca und niiscular thickeoing

absent, Exerelory system meronephric. Puired

tufts present in FT. TI-V of which at feast

those in IV and VY are enteronephric, with

ducts entering the buccal cavity and/or the

pharynx, Caudally with numerous entero-

nephric meronephridis. euch with a preseptal

funnel, dischatging into the intestine in each

segment and with or withoul a longiludinal

collecting duct (ureter? on cach side. Testes

and funnels in X and Xi: tustis-sucs absent;

seminal vesicles in XJ and XIL or rarely th

1X, XL and XI.

Ovaries and [unnels in XU; avisucs present

or absent, Prostates tubuloracemuse: liner,

lobulated. with axial himen throughout which

receives lateral canaticull; vas yleferens join-

ing their muscular ducts, Penigl setae ubsent.

Spermathecae with diverticula,

Type-species: Geniayeoler newmant Edmonds

& Jamieson, 1973,

Disiribution: South Astralia and Victoria.

CHECKLIST OF SPECIES

*New combinations in Gemascolex

South Australia;

1, Gemuscolex bursarus sp. nov.

2, Perichaeta Jateralis* Spencer, 1892 (also

Victoria), syn. Megascalex zietzl Michael-

sen, 1907b

3. Gemascolex tirabilis sp. nov.

4, Gemascolex newmant Edmonds & Jamic-

son, 1973

5. Gemascolex octothecatus sp, nev.

6. Gemascolex similiy sp. nov.

7. Perlehaera stirlingi* Fletcher. 1R88a, syn.

Megascalex fletcheri Shannan, 19206

8. Gemascoley walkeri sp. nov.

Victoria:

9, Perichaeia dorsalis® Fletcher, )BERb

Gemascolex bursatus sp. nov.

FIGS 3A, 10C, 11B-E; TABLE 4

Length — 52(P1)-64(H) mm, w (mldclitel-

lar) > 1,S¢PL)-2.5¢H) mm, s = BIPI-

102(H), Piemerted purptish-brown dorsally,

pale ventrally; setae in pale circular fields.

BR Rh. Ci. M. JAMIESON

TABLE 4

hitersetal distances in Gemascolex bursalus

@andarelieed a5 Fr

mm of circumference

Bp abo o= a2 u oy oabovy ca

Seanent XU

Holowre 0.6 04 04 05 $2 122 7H 74a [NF

Pafotype t ba U3 04 04 62 B84 60 71 101

Mean 104 54a TS WT

tntorval/ab 15 10 77 O18

Sesment XX _ _

Halowpe 07 Os 04 O03 58 18 32 75 140

Paratyoe | 06 0.3 63 05 46 i564 45 AG lA

Mean 13.2 75 71) 323

Tntervalab L7 tO OF be

Prostamum tanylobous. harrow, acute (IN) or

epilobous, 3/4, open, Camalicula absent. Dor-

sal pores minute, the dirst in 4/5. Setae of each

sidé mure closely spaced luterally than dor-

sally and ventrally; ab and be approximately

equal, Numbers of setae per segment L8 in

XII, 16 in XX (H, PL), 20(P1}-22(H) Ail-

teen segments from the cyudal end; @ and 2

lines straight throughout; anteriorly with a

wide break in the setul circlet dorsally and

ventrally; posteriosly with a moderate ventral

and almest inupprectable dorsal break. Setae

a and } but not ¢ absent in XVILL Clitellum

(developed in holotype only) XTM-XVL (= 4

segments). Male pores extensive transverse

slits, with puckered lips bul 90 porophares, im-

mediately median to setae ec of XVIII,

1.05(H)-L.30¢P1) mm, 0.29(P1)-(.381H)

circumference, apart. A circular, low dome-

shaped accessory genital marking present al

17/18 and 18/19 in Front of and behind the

male pore, on the left side, but at 18/19 onty

an the right side (UL): paired in these locations

in Pl. A pair of elliptical eyelike markings in

16/17 in ab (FE only) and a Further pair of

circular to elliptical markings in 8/9 slightly

lateral of A lines (11, P1); all accessory genital

matkines vudimentary in Pl. Spermathecal

pores 2 pairs, in 7/8 ancl 8/9, laterally situated

vaping clefts, shortly lateral of setal lines 4,

L.32¢H)-—20(P1) mm, MaR(P1)-0.56/H)

circumference. apart.

Strongest septa 9/70-13/ 14, inoderately

strongly thickened. Last hearts in XU, Supra-

oesophaweu! recognizable in VII(H},

VOI PIy-4 XIN PL), XUT(H), well de-

veloped. Gizzard in V. Intestine originauliig. in

XVEIT in which it resembles the vascularisesd

regions of the oesophagus; 4 low Lorruous der

sal typhlosole first considerably developed in

XXVIII but traceable forward as a rudiment

to XXIII. Nephridia: a pair of tufts tn each

of segments I-V, inercasing from small to

large posteriad, those in IY ynd VY sending

composite ducts to the pharyna; those in JT

and TIP apparently exonephric, smull cxa-

hephric tufts in VI accompanied laterally by

jicromeronephridia (H, PL); numerous in-

legumentary micromeronephridia in VIL pos-

teriorly, at first posterior in their segments (F,

Pl), in XVI-EXVUL especially conspicuous and

densely crowded on the body wall (H); there«

after (Tf, P1) moderately numerous on each

ste and posterior in. cach segment, caudally

with several fis many as 8 er 9) enlarged

nephridia an cach side with a preseptal funnel,

at least some of these nephridia On each side

sending ducts to the roof of the inlestine;

accompanied in the holotype by smaller asto-

mile, (exonephtic?) ocphridia; no ureters

demonstrable, Precise descnption of the

nephridia nrust be postponed until more appro-

priately fixed material is available.

Sperm funnels in X and XI (iridescent in

the mature holotype; seminal vesicles race-

mose, in XI and XII. Ovanes oval laminae

with several large oocytes. (H), rudimentary

in the paratype: accompanicd mediunly by

small sacs of unknown function, ovisacs

present. Prostates tubuloracemose, cuch with

flattencd leaflike glandular portion, in XXTT—

XXVI, XXVTI, deeply incised by the septa

and adherent to the intestine: the muscular

duct strvight in XIX—XXIT but in MVE carv-

ing medianly around the anterior Face of a

large subsphericul bursa copulatrix. A tonicul

penis-like structure projecting from the bursa

into the male genital aperture though not

visible externally; vas deferens joining the

junction of prastale duct and gland (H); pros-

tate glands rudimentary jn P1.

Spermathecae 2 pairs, in VINE and TX: duct.

ampulla and diverticulum tortuous, the diver-

ticulum (inseminated) slender, tubular, uni-

loculate, a little larger than the ompulla CH);

spermathecye rudimentary in PL.

Material examined: Jj3, 138°30B, 35°22",

hill & km from Myponga, S falinends,

(6.viiil.1972-H(AM), P1( BI).

Remarks: The muscular bursae at the ectil

ends of the prostate alucts in this species are

um@que in the genus,

Gemiascolex lateralis (Spencer, 1892)

FIGS 4A, B, 10D-F, 11F; TABLE 5

Pevichaeta lateralis Spencer, 1892; 11-12, PI

VI. figs 55-57, 78,

Meeascalex lateralis Michaelset,

Jamieson. 197 Lb: 95,

Megascolex zietsi: Michaelsen, 1907b;

Jamieson, 1971b; 95,

1900: 230,

7-19.

EARTHWORMS FROM SOUTH AUSTRALIA 89

XVI

XVII

XIX

A in

Fig,

The following account is drawn from the

lectotype, two specimens. from locality Ji2

(SA77, 79). a specimen from LI] (SA15),

and one from Lk3 (SA229). These are re-

ferred to as L, and specimens 1, 2, 3 and 4

respectively in the account.

Length = 45 (specimen 3), 74 (specimen

2)-80(L} mm (specimens 1 and 4 are pos-

5p.p

3. Genital fields of: 4, Gemascolex bursatus, holotype, Jj3. B, G. similis, holotype, LI2,

terior Tegencrates), w (midclitellar) = 3-4

mm, s — 87 (specimen 3), 109 (specimen 2)~—

122(L). Circular in cross section. Pigmented

purplish brown dorsally with the setae in pale

fields (specimens 1 and 2); or pigmentless

(bleached?) (L; specimens 3 and 4). Pros-

tomium epilobous 1/2 (specimens 3 and 4)

and 2/3 (specimens 1 and 2) or appearing

ue B. G. M

TABLE $§

fniersvpad distances in Gemascolex luteralis

Spandardived zs S

min of citcumfterence

us ooab zy 77 ” aoa cy ee

Seement Xft

13a TT if oe OF Ll ils $4 46 Gl aa

25a 75 10 BS Oo baie 6S 6h gf WS

JSA 15 on 0A Of O89 TS 7,2 4.0 3.6 11.3

45a 229 07 D4 BS 9 Bz 76 44 54 92

Seument 4X

13SA 77 13 05 HS Lain w4 45 44 484

258A 74 14 04 O68 F2T3L J07 59 4h BY

3 SA 1s 10 @S UA TL O25 ws £3 18 JIN

45A229 1 O85 GS J FS 14 SS $3 157

tranviobous (LL); sor ur faintly canaliculate.

closed or open. First dorsal pore 4/5. Setae

more closely spaced ventrulaterally than doc-

sally and ventrally on cach side; ab signifi-

cantly, but not greatly larger thin fe in most

yeements: numbers of setae per segment 21-

31 (meun of & 26) in XU, 17-24 (mean

of 5 = 22) in XX. 20-38 (mean of 5 2A)

fifteen scuments From the caudal end: a dis-

tihet thourh odnly moderately wide ventral

hreak present throughout, a dorsal break

present in the forcbody but behind the clitel-

lum only initially recognizable. of present bur

narrow throughout. Sctac «@, A and ¢ ybsent in

XVOT of (L) a and }, only absent.

Clitetlum MIM (specimens 2-4). XIV (Es

epecimen 1J-XWVI (L, specimen 1, 2), 1/5

XVIT (specimens 3 and 4) [> 3-4 1/3 seg-

menis), Mile pores on prominent rounded

porophores ine lines of XVUML. distance apart

2.04 [specimen 3), 2-81 [specimen 4),

Jl (LL), 4204 (specimen 1}, 4.92 (specimen

2) mm: ratio of this lo circumference —

0.26 (LY, O:.30 {specimen 4). 0.31 (specimen

3). 0.33 (specimens | and 2), Accessory

venital markings, & pair of evelike markings

in cach of intersegments 9/10 and 10/11 ia

ah (Ls specimens 1+). Additional markings

in 17/18-212 22, varying From a@ lines at b7/18

to slightly median of w at 21/22 (1), or tn

17/ 18-22/25 (specimens | and 2) or absent

(specimens 3 und 4). A further pair of sub-

circular niarkings present in NXVILE in frone

of the male pores (L: specimens 1-4) and a

second pair behind them {specimens 1 anil 2)

fsee Piel) Variation}: Spermathecal pores 3

pairs. clearly visible sunken orifices or incan-

spicious, ifn 6/7-8'9, hetween setal lines 4

and 3; distance between pores = 2.04 {speci-

men 3). 30 (specimen 4), 4.5 (lectotype>,

4.92 (specimen 1). 5.62 (specimen 2) mm:

ratio of this distance to circumference = 0.24

(specimen 3), 0.34 (apecimen 41, 0,35 [lecto-

type), 0,39 (specimen 2), {1.42 (specimen 1),

‘AMIESON

Several pre-intestinal septa: thickened but

none strongly. Jast hearts in XIE. Supra-

oesophageal vessel in 1/2 VITI-1/2 XILL well

developed (specimens 1 and 2); ill-defined in

specimens 3 and 4, Vascular sysfem not intact

in the lectorype. Gizzard in V, Inteslinul origin

XVI; a very low, rudimentary. dorsal typhio-

sole first definitely recognizable in XAXVIL

Nephridia: small paired tufts in dt and Jil

with anterolaterally directed compesite ducts

which in specimens 1-4 appewr to be

exonephric but in the Jectotype join the buccal

cavity at ats anterior limit. Large tufts im VV

und V enteronephric. their composite ducts

running anteromediplly to join the phiurynx.

Numerous exonephric astomate micromero-

nephridia present in | or more bands in V

posteriorly (visible from IL] in specimens 3 and

4), associated with the anterior anil posterior

septa in XV {specimens | and 2) or XVII

(specimens 3 and 4) posferiurly, Caudally

with approximately & enlarged nephridia. each

with a preseptal Funnel on each side; ome or

Iwo hephri¢inl ducts traced to the rool of the

intestine but prohably all enteronephric: ro

longitudinal collecting duets demonstrable

Sperm funnels iridescent in X and XI; seminal

vesicles Slightly racemase, almost sacciiorm, 2

or 3 pairs, in 1X (Lh, specimens | and 2), XT

and XIF fall spectmens). Ovaries, Natrened

webs or lobes with several conjotned strings of

large oocytes, and funnels; a crescentic sac

of unknown function seen on the anterior sep-

tum of XI[L median to the ovaries in che leotn-

type and specimens | and 2: sacs on the an-

ierior septum of XIV questionably ovisacs.

Prostales tubuloracemose, hand-sectians of one

of spectmen 2 revealing a very natrow ceniral

lumen; the broad glandular portien linet, in

XVIUEXXIF XXIIL deeply incised) by the

septa: the musculur duct forming a Joop at

leust the cetal limb of which widens strangly

hut a copulatory bursa absent: the vas deferens

joining the duct near its junction with the

eland. No glandulir miusses distinguishable in-

ternwily ul the sites of the accessory genital

miurkings Spermathecae 3 pairs, diverticulum

(inseminated) single. twhwlar, very lang and

much coiled,

Field variation: Anterior genital markings are

commonly absent in specimens with well

developed markings in the vicinity of the male

genital field. When anterior niarkings are

present they usually occur in 9/10 and 10/ tt

but they sometimes are present in 1/11 ante

und carely in 8/9 only, there are rarely 3 pilirs,

EARTHWORMS FROM SOUTH AUSTRALIA of

Fig.

in 8/9, 9/10 and 10/11. A pair of markings

is invariably present in XVIII in front of the

male pores and a further pair is usually

present behind the pores. In no specimens are

the posterior markings present in the absence

of the ynterior pair,

Paired intersegmental genital markings in

the vicinity of the male pores may be absent

4, Gemasculex lateralis. Genital fields of: A, specimen }, Ji2; B, specimen 3. Li,

but they are usually present in 18/19, 19/20,

commonly in 20/21 and 21/22 and less fre-

quently m 17/18 and 22/23.

In all but one of the many specimens

examined. the female pore was unpaired.

Material examined: Ig\, 138°03'E, 32°46'S,

Alligator Gorge National Park, under rocks

negr Creek in gorge, BJ. and T.W.,

02 B. G. M. JAMIESON

19, viii, 1972—SA 26-30, 33. $h2, 138°38'E,

33°55'S, 10 km & of Clare on road to

Auburn, under eucalypis, &J. and TM,

8.vill, 1972—SA (65, SA 170, SA 318, 319,

JiZ, J38°24'R, 34°5R'S, Mt, Lofty, Tor.,

16.viii1972—SA 306 Mt Lofty. in cucalypl

wooWland, BJ. and 7.W., 16.vii.J972—SA

289-296, 298, 299, 301-302, 304, 305; M1,

Lofty area, in morst sotl in eucalypt scleco-

phyil, TW. 20.viii.L972—SA 77, 78, 79, 82,

RI. Jil, 138°41'E. 35°07'S, Mt. Bold reser-

voir, on hillside with eucalypts and griss,

TW, 21viil. 1972 SA 57-60. Jj2, 138°43°E,

34° 14'S. Kyeema National Park, near creek

and under logs in cucslypt sclerophyll and

in swamp, T.W., 21.viii.1972—SA 271, 279,

2ho, 287. Jj3, 138°30'R, 35°22'S. 6.5 km

from Myponga, §. Edmonds, 16.viit,L972—

SA I3h, 237. Jj4, 138°30B, 35°26°S, near

Mt. Clark (S of Mypongal, eucalypt

sclerophyll, T.W., 21.viit, 972—SA 64, 69-

72. Jj5, LSS" bt E. 35°36°S, 8 km from Cape

Jervis along road to Victor Harbor, in grass-

trec, bracken and eucalypt bushland, T.lW.,

WiLL EYT2—-SA 285, 2H7. Jj6, 1398°21'E,

35°34'S. 24 km from Cape Jervis along road

tw Vietor Harbor, under rocks and logs in

poor soil, 7.4, 21 viii,1972—SA 207, 209,

21, 215, Jp?, 138°25°E, 35°33'S, 30 km

from Cape Jervis along road to Victor Har-

hor, in grasstree and eucalypt mulga, 7'.W..

21 viil, L972—SA 172, 176. Jj8. 138°32’E.

35°34°8S, 10 km from Victor Harbor to Cape

Jervis, under roadside fog, T.H’., 21 -vili.1972

—S 42 (invmyture). Kyl, 239°2S8'E,

35°15'S, Tailem Bend, under rocks on bank

of the Murray River, AJ, and 7,6,

WOviiLIO72—SA 1RB-19D, 192-193, 105-

WI, 203-205 Lk3, 14N*3R'E, 34°42'S, 32

km from Naracoorte to Bordertown, in

sundy sail among Banksia, gums and

bracken, BJ. and TW, 16.viii.1972—SA

219 330. LID, 140) 49°R, 37°28'S. 11 kim S

of Penola at roadside. under cucalypts fring-

ing Pinus radiata, «= RS. and oT,

1S.vii 1972—SA 15. LIZ, L40°32'B.

37°41'S, 18 km SE of Millicent on toad to

Mt, Gambier, in sandy soil with fErass,

bracken and Drasera fringing a Pinwy radiata

plantation, F.W. IS.vii t972—SA AT

SA 15, 79 (AM); SA 77, 229 (BM); SA

289 (SAM); the remaining specimens (BI),

Remarks: Examination of the lectotype of

Perichoeta lateralis reveals Ue presence of

paired genital markings, overlouked by Spen-

cer, 1 9/10 and 10/11 and does not confirm

palnog of the female pore reported in his

description. Agreement of the new material,

and Michwelsen's deseripliun of Megaieoles

rierze, With the lestotype is so close as to allow

no doubt of conspecificity.

The possibility that an infraspecific morph,

subspecies. or, less likely, a sibling species

should be recognized for at leust same popu-

lations which have gemisl murkings on XVII

both behind and in front of the male pores

deserves jnvesligation. In such specimens

(exemplified by specimens 3 and 4) the male

spermathecal pores, allhOugh an the same setal

lines as the typical morph. (cxemplificd by

the lectotype and specrmens | und 2} ure

usually closer together transyersely, The sper-

mathecal diverticula are, so far as inyvestivuted,

shorter and less convoluted. Furthermore.

paired intersegmental genital markings jn ihe

vicinity of the male pores may be absent

though frequently present The occurrence

sympatrically on Mt. Lofty of specimens with

or without markings behind the male pores,

in addition to those in front, at present mili-

tates against recognition of subspecies, How-

ever, it is hoped that 4 statistical examination

of morphology in pepulations of G /ateralis

and of theit biology will be undertaken hy

workers in South Australia with a view to de-

termining the status of the variants mentioned.

G_ luteralis is the only indigenous megas-

colecid, other than /feteroperodrilus shephardi,

kiewn to occur outside South Austrulia Cin

Victoria)

Gemuscolex mirabilis sp, nov,

FIGS 3. 10G; TABLE 6

Lenghh = 60¢H)-83(P1) mm, w (mid-

clitellar) — S.5(H)-+.9fPI13 mm, » =

L20(P1}-128(H). Circular in cross section.

Pigmeniless with the exception of the brownish

glitcllum. Prostomium epitanylobaus. closed at

1/3 peristomium and laterul borders to O/T

not certainly distinguishable from longitudinal

furrows on the peristomiam but bisected by a

deep canalicula to 0/1. Peristumium longitud-

inally grooved all round but not bisected ven-

trally. First dorsal pore 3/4, fimperforate?,

Pl), 4/5 (H, Pl). Setae subequally spaced.

though oc is slightly wider than af throughout.

Numbers of setae per segment 20(P1}—21(H)

in XU, 2)¢PT)-220H) in XX, 20(H)-21(P1)

fifteen segments from the caudal end; a@ lines

straigh| throughni; 2 lines straight anterior to,

irregular posterior to the clitellum: a ventral

EARTHWORMS FROM SOUTH AUSTRALIA 9

TABLE 6

intersetal distances in Gemascolex mirabilis

standardjrod an %

mito of circumference

a abo oay ma u aa oahooay we

Segment NIT

HoloWne 1.0 Ua O7 15 125 7.6 IN 59 14

Paidtyoe 12 06 68 47 157 74 40 5.4 105

Meun 75 38 SS. 4

Imtereal/ab 2.0 i 1.4 3.0

Serment XX

Holotype O7 04 12 £9 13.9 44 25 6.6 17,9

Paratype | 14 06 10 2 17,6 80 3h AK Wi

Mean GJ 3f 72 125

Interval ‘ub 72 10 24 41

and a dorsal break present throughout. Setac

acand #, but not ¢, absent ia XVIT,

Clitellum: XTA(P1), 1/ 3X1 H)-X VIC),

L/3XVUN(PL) (= 4 2/3-5 1/3 segments),

Male pores minute Jongitudinal slits in a near

the median borders of a pair of large poro-

phores; the pores 1,40(H)-1.79(P3} mm,

6.09(HI—-0,10( PL) circumference upurt,

Accessory genital markings paired transversely

elliptical tumescences, with slit like centres, ex-

tending from lateral of ¢ to median of 4, in

16/17(P1), 19/20, 20/21. PIL), 21/22 and

22/23(H), Spermathecal pores 2 pairs of small

pores concealed in 6/7 and 7/8, in ab, nearer

a, With a faintly demarcated lip in front of each

on the preceding segment; the pores 1,37(H)—

1.72(P1) mm, 0.09-0.11 circumference apart.

Steongest septa 9/10-12/13, moderately

strongly thickened. Last septal glands in TV,

not javelving the gizzard. Last hearts in XIE

connectives in X-XIM from supra-ocsophugeal

larger than the dorsal connectives and each

jomed before it reuches the latter vessel by a

vessel from the corresponding side af the

oesophageal Wall. Supra-nesophagesal in X—

XIU, weakly developed despite jhe large size

of the connectives to the hearts. Gizzard in V,

Ocsophagus almost suppressed to VIEL and

short In TX owing to backwards projection of

the gizzard; vascularized (though not con-

spicuously) and dilated in X-XITIT, with high

internal villi almost occluding the lumen but

not, uniting axially. Intestinal origin XVI: a

well developed, though tow, tortuous dorsal

typhlosole commencing jin XXV(P1Y or

XXVI(H). Nephridia: a large pair of tufted

nephridia, with inoumerable spiral loops, in VI

sending several composite ducts anterolaterally

aul anteromedially to ihe body wall anteriorly

in this segment; an extremely large pair of

tufts in V sending composite ducts to the

pharynx and additional tong composite duets

fur forward to the vicinily of interseament 1/2.

Very stall pharyngeal tufts.in TV (H, Pl) a

. Gerascolex mirahifis, Genital field. holo-

type Jez.

rudimentary tult on each side in LICH); none

detectable in ICH} or in Il and BI(PL).

Lateral bands of astomate, exonephnc micro-

meronephridia posterior in their scgments in

VII-XU(H), XUICPT) then becoming pro-

gressively more anterior until in XV(PL) or

XVI(H) they are attached to the anterior sep-

tum, the bands especially dense jin XTII-

XVI: in the anterior intestinal region with

approximately 13 compact ustomate micro-

meronephridia on each side dependent from

the anterior septum but exonephric, Caudally

with approximately 8 enlarged nephridia on

each side, closely udjacent to and encircling

the intestine fromm almost the middorsal line

laterally; each with a large, long-stalked pre-

septal funnel; these nephridia sending separate

ducts medially to unite as a common duct

which passes diagonally, posteromedially,

heneath the dorsal blood vessel on each side,

to enter the body wall posteriorly in the seg,

ment; the diagonal duct on éach side com-

municating by a narrower duct with that of the

a4 B, <i, M, JAMIESON

neat cumeent seainents, Numerous astoniute,

appurently exonephri¢, s¢ptal micromera-

nephridja preset at the parieies, surrounding

and concentric with the enlarged, enteronephnc

nephridia (1H, P1}. Sperm funnels weakly iri-

descent in X and Xt. Seminal vesicles rage-

most. in XL and Xi! Ovaries composed of

several partly united strings of Jurge oocytes,

Flattened’ saclike structures in XIV may be

ovisies. Prostates tongue-shaped, restricted to

and passing Inteealty in XVIIE, incised once

to IWice xo 48 16 sugeest a muulified. depressed

tubulac Jorm CH, P21); with a narrow central

lumen throughout which has cpithelivm-lined

side brunches (schizeparatype); the muscular

ducl widening significantly towards the pore

ant joined near its ental end by the vasa

deferentia, these sale ducts running separately

from each other in the thick muscular wall

of the prostate duct near the lumen of the

latter. but not penetrating the lining epivhelium

to join the lumen until the male pore is almost

reached (schizopuratype); copulatory bursa

absent, Spermathecue 2 pairs, in Vit and VIII.

the single diverticuluny subspherical, sessile,

with several internal inseminated loculi, ibe

dict inflated, spindle Shaped (H, P1_ schizo-

paratype}.

Field veariatiany In 11 clitellate type-specimens.

including the holotype, genital markings are in

15/16 (left) in specimen (P10), 16/47 in 6

(5 paired, 1 mghe): 19/20 and 20/21 in 1

(all paired in 19/20; unilateral right or left in

2 in 20/20): 21022 in 2 (! paired, | rightl:

and 22/23 in 1 (paired). The male porophores

i some specimens sire surrounded By a com-

mon, medianly narrowing field taised at its

edges usa rimlike tumescensce which ts closely’

udjucent to the lateral borders of the poro-

phores

Material cacbtined: Jg2, 138°10'R, 32°48'8.

Mt. Remarkable, on slopes of mountain in

rocky sil covered with animal fwallaby?)

droppings, BJ. and T.W., 18.viii 1972—H,

PI-10. Pil (schizopyrutvpe): many other

‘specimens collected but wot designated type-

specimens, Jel, 138°03°E. 32°46'S, Alliga-

tor Gorge National Park. under rocks near

creck in goree, BJ. ond TW, 19.vili 1972—

Pi2, H, P2-5 (AM), Pl, P6 (BM); P7—

& (SAM): P9-12 ond others (BJ).

Remurks: location of the two pairs of sper-

mathecal pores in 6/7 and 8/9 and the con-

figuration of the genital markings readily dis-

tinguish G. xifrabiliy Prom other species.

Gemascolex octothecatus sp. noy,

FIGS 64, RB. OH, 1; TABLE 7

Length 45(P11-b4(H) mm. wosimiu-

cliiellar) — 4.7-54 mm, s 7L{P))- 84H)

(posterior regenerates?), Generally circular in

cross section but the ventral surface somewhat

Nattencd at and anierivr to the male genital

field. Pigmented purplish brown dorsally,

coloriess ventrally, in alewhel; euch seta in the

pigmented areas surrounded by a colortess

circular field, Prostomium nol canvliculate (A)

or with weak dorsal canalicula (PI), epilobous

1/3(HI-1/2¢P1), closed by » deep transverse

furrow bul continuing posterior as an acille

(H) or parallel-sided (Pt) tongue which

almost reaches the first intersegment, First dor-

sal pare 45, Setac of each side more closely

spaced laterally than dorsally und ventrullys «>

significuntly lurger than ec, the setae of the

ventral couple more conspicuous thin others.

Numbers of setac per segment 20 in XINH,

Pl); 1RCP19-19(H) in XX: 2ZO(PLI-2SLH)

filleen segments from the caudal end; 2 lines

straight, z lines irregwlat; a wide ventral and

dorsal break in the setal circlet present Lhrough-

oul. Setac uw, 4 and ¢ absent in XVLIT in the

prostutic holotype but present in the aprostauc

paratype |,

Clitellum XILUCH), XIVEPT)—F/ 2X VET dor-

sally (3 1/2-4 1/2 seements) annular ful

ventrally (H) weakly developed in XIE and

appurently not developed in XVII, iitterseg-

mentul furrow 13/14 well demarcated ven-

trally (though not dorsally), the xuceceding

furrows weakly indicated; dorsal pore 13/14

Well developed. 16/17 partly oeclided, the

others obliterated: setae « and / elearly vistble,

the remainder only sporadically visthle (11)

Male pores jninvte. on stump-like, annilated

pseudopenes. in ce of XVI, which are

strongly protuberant from gaping slit-like str-

rounding basal areas which may represent the

male pores before eversion of the pseudopenes,

the basal slits each horne on a large annulated

porophore: the bases of the pseudopenes 6.4

rim, 0,35 circumference apart (H). Male pores

and porophores totally absent in paratype 1.

Accessory genital markings paired with pore-

like centres, presetally in X in 4; in 16/17

centred in or slightly median of &: in 17/18

und 18/19 slightly lateral of b; and in 19/20

gad 20/21 slightly median of CH, see Ficld

Variation). Spermathecal pores 4 pairs, in

S/f, 6/7. 7'°S and &/%: in a straight line on

each side but between setal nes 4 and & in

5/6. and between @ and 7 jn 8/9, distinctly

EARTHWORMS FROM SOUTH AUSTRALIA 95

TABLE 7

Interseral dismmees dt Gemasealex oeteihaealus

Ee ne

Hanlurizest ay Vp

mm of ¢ircumicrence

xr aa mb zy be u woabo xy ®&

CRUNCH

hy alate '7 J0 O07 as i78 95 56 40 40

Paratype ( LL O83 U6 1214 82 SA 45 60

Mean 8.9 3.6 4.3 [LS

Toverpal/ah 16 10 98 ay

Seeniont X

Hotowne 7 Jv 1H 2643.5 92 60 £4 140

Pafaiyre: 1 11 OR O68 bs 444 TA 43 43 92

Meso #5 S77 AM 116

Interval/ab 15°18 D4 BL

ee ee

visible small whitish oval puplilae confined to

the intersegmental furrows; in 8/9, 7.7(PL)—

9 O(H) min, (1.57 (HI-O.58(01) cireurference

apart, 7.e, slightly dorsal (H, PL),

Strongest septa 11, 12-13/14, moderutely

strong, Last hearts in XI1, Supra-vesophageal

vessel in VIR 1/2VEL-1/2X011, well

develuped. Heals in V. VIT-IX dorsoventral

only, thuweh still valvulae giving branches to

septa and body wall. unlike the more posterior

heurts. Giazard in VI Intestinal Ongin XVII;

iw very low. Sairly broad dorsal typhlosole com-

mencing tm XIX, Nephridia: a pair vt large

tults. with many spiral loops in each of sep.

mens JI-V, imeressing in size posteriad, to

very large in V; the tufts in IL and JEL send-

ing Lomposite ducts forward in common to

juin the body wall near the buccal cavity and

into the peristomium where they possibly enter

the buceal cavity; those in IV and V dischurg-

ing into the pharynx, Meronephridia parictal

und apparently exonephric in transverse bands

in VE posteriorly; caudally, from upproximately

the 50h segment with 8 or more long-necked

preseptal funnels on each side and with the

median 2 of these stomate nephridia enlarged

as Megameronephridia the 4 of which lie on

the dorsul surface of the intestine and send

therr ducts to the intestinal walls the evo ducts

Wniting on each side of the dorsal vessel, and

in continuity with thase of neigitbouring seg-

menis: the longitudinal duct apparently but not

tertuinly opening inta the intestine posteriorly

in cach segment. Laterally the nephridia be-

come progressively smaller. though each re-

fams a preseptil funnel; they ace dependent

from the anterior septum and sone at least

send ducts to the roof of the intestine and are

apparently also enleronephric. Elungate lobed

testes and large complesly folded, pearly but

NOL ividescent sperm funnels in X and XI; 2

or 3 pairs of moderately large sacciforny sem-

inl vesicles in IX(H}), XI and XIU (H, P1).

Prostites large, broad lobed structures ip

NVUI-XXI (tft), —XXU tight), each deeply

metsed laterally and less so medianly by the

septs; the (\-shaped muscular duct entally

AATFOW. Widening strongly and uniformly getul-

wards hut lacking a Lerminal bursa; Vas

deferens joining it near its junction with the

gland (H), Large, paired. low internal glandu-

Jar snasses in XVI-XXi corresponding with

Cxtemul accessory eonital markings (A, PI).

Prostates totally absent fram Paratype | al-

(hough the specimen is mature; ectal portions

ol vasa deferemia noi observuble. Ovaries

(bushy with many large oocytes (PL) or

poorly develuped (H)) and funnets in XIIL,

accompanicd medianly by sacs of unknown

function; sacs on the anterior scptum of XIV

may be ovisacs, Spermathecae 4 pairs. diver-

liculuny single, elongate clavate, uniloculate.

shorter (Pl) or longer (H) than the sper-

matheca, sumelimes coiled,

field varition- OF the 6 lype-specimens, only

the holotype has male pores: 3 of the pari-

types dissecled. | of which is longer thun the

holotype and fully clitellute, have na prostate

glands, Puired accessory genital markings an-

leriorly in X in } lines are invariably present

as are paired markings in 16/17-19/ 2th They

are present in 20/21 in paratypes 1 and 2, as

i) the holotype, Additional paired markings

are present in 15/L6 in paratype 3. A ruui-

mentaty marking is preseat unilaterally on the

right, in [2/13 in paratype 4. In specimens

lacking inale pores the genit:| markings in 19/

1818/19 sre dightly more median than in

the prostwtic holotype, lying in a neurer b,

Tather than in & lines,

Material exainined: Lil, 140°49°E, 37°28'S,

11 km S of Penola in cucalypis fringing

Pinus radiate, BJ. and PAM, 15.viii.1972—

Pl, Lmt, 140°5S'E, 38°OL'S, 27 km from

Mi. Gambier along roau to Nelson, in sandy

loam under grass among watdes and gums

with some herbaceous garden escapes, BL,

and TW. 15,viii.1972—H, P2-5, H, p2

(AM): Pl (BM): P3 (SAM): P4 & § {B]}.

Remarks: G. actoshecatuy resembles G. dorsalis

{Fletcher}, from Vietoria, in possessing four

pairs of spermatheeae and in the dorsal loca-

tlon of their pores, A further similarity be-

tween the two species is the pair of genital

markings at the anterior margins of X and

XVIL. G. dorsalis differs, however, in restric-

lion of genital murkings to these locations in

all localities from which it has been reporied

(Fletcher I888b; Spencer 1892- Michaetsen

19076); and in the more dorsal location of the

96 B. G. M. JAMIESON

Fig. 6. Genital fields of: A & B, G. actothecatus, A, holotype, Lm1; B, paratype 1, Lil. C, Pertony-

chella (P.) inconstans, holotype, Mjl.

EARTHWORMS FROM SOUTH AUSTRALIA a7

spermathecal pores. G. similiv differs fram tt.

octolhecates in the smaller number of sper-

mathecal pores, restriclion of wecessory genital

markings to X, 76/17 and (8/19. and the

greaier development of these markings. These

Uifferehees of G, verothecarus from G_ dorsalis

und G. sivuvfiy sre minor compared with those

between ether species of the genus but union

of the three entities in G. dorsalis nevertheless

does not appear justified,

The prevalence of individuals Jacking male

lerminalia suggests tha} G. voctotheraus is

commonly parthenogenetic.

Gemascolex similis sp. nov,

FIGS 38, 10), K; TABLE 8

Length = 40 mm + (posterior amputee),

w (midclirellar} = 4.5 mm, s = ?. Pismented,

purplish brown, dorsally, Citcular in cross sec-

tion, Prostomium cpilobous 1/3, closed. Pre-

clitellar setae large. postelitellar indistinct,

setae of a side more widely spaced dorsally

and ventrally than between, decreasing in size

dorsally; wb slightly wider than be throughout.

Numbers of setue per segment [8 in XU and

XX_ 20? (indistinet) in NXXY; a lines straight,

t lines irregular throughout; a wide ventra)

hreak evirent throughour; dorsal break wider

and clearly visible anterior to the clitellum,

poorly defined behind it owing to minutencss

and irregularity of the setae: a and 4 absent in

XVI, co and d faintly visible on the lateral

face of the jrophore,

Clitellum rudimentary, apparently occupy-

ing XIV-1/2 XVI (— 3 1/2 segments), pot

sulfictently developed to obscure dorsal pores,

intersegments oF seiae, Male pores minute, on

sluimp-like, annulated pseudopencs, median to ¢

of XVII; a hasat circumferential groove

around each pseudopenis may represent the

margins of mele pore before eversion of the

mseudopenis, this basal groove is itself borne

on a large unnulated porophore; the centres of

the bases of the pseucdopenes 4.8 mm, 0,33

sircuniference, apart, Accessory gemital mark-

ings. pilited subelrevlar, butlunitke. sharply

demarcated lumescences, cach differentiated

into a penpheral ring and flat or depressed cen-

Ir arca. filling the presetal part of X in 4:

in 16/17 and 17/18 in eh, filling the spnce

between the setal arcs of the adjacent seg-

ments, these 7m 16/17 more median than those

17/18. Female pore unpaired. midventral in

XIV, preseral in jin elliptical field, Spermathe-

cal pores 3 pairs. In 6/7, 7/8 and 8/9, incon-

spicuous Whitish ellipses, In selal Hines 5-6,

TABLE 8

litersetadl distances in Geniascolex similis

srindardized as %

antn uf elreun ference

ga oats vy ow u Ma uh oy ?

Soetiont XT

Holotype 17 09 09 Thi 72t Gt at ie

tneerval/ab 20 10 Ly 2A

4-5 and 5-6 respectively (right sive, not cer-

tainly visible eaternally on left side); 9 mm,

0,54 circumference apart, ic, slightly dorsal,

Strongest septa 10/11 and 11/12, very

suong; 8/9, 9/10, 12/13 and 13/14 also

strong. Last hearts in XIII. Supra-cesophageal

Vessel in IX-I/2 XIII; moderately developed.

Gizzard in V1, Intestinal osigin KVII, a very

law sidgelike dorsal typhlosole commeucing in

ipproximately XVII. Nephridia: paired tits

in 1-V, increasing posteriad from small to

large: those in TI and UN discharging

exonephnically anteriorly in their respective

scgments; those in IV appurenily, but not cer-

tainly, discharging into the pharynx; those in

V each with 4 wide composite (multiple) duct

running anteromedially to the pharynx wall in

il. Numetous exonephric micromeronephridia

mostly in posterior bands in their segments in

VI-XITI: mastly presetal in XII; anterior and

pusterior bands of micromeronephridia in

XIV-XNJ; thereafter mostly anterior jn each

vegment; no nephrostomes present but pos-

lertor end missing behind the 40th seement.

Sperm funnels iridescent in X and XT; semi-

nil vesicles saccular, in XL und XU; 4 pair of

small sacs on the anterior wall of X resenible

seminal vesicles but in this locwtion presumably:

ilo net have a seminal function, Ovaries with

several chains of large oocyies, small Aattencd

sacs on each side of them; ovisacs absent.

Prostates large flattened lobes, with irregular,

lobed, moderately deeply inciscd margins,

restricted fo but greatly enlarging XVII:

the tortuous muscular duct gradually but

considerably widening through jis length

to the pore. Large intraceclomic gplandolar

masses amt associated with the accessory

genital markings. Spermathecae 3 pairs,

approximately uniform in size: diverticulum

[inseminated) single, digitiform, but that of

the lefl spermstheca of LX with a trileculate

terminal dilatution.

Material exaniined! LIZ. 140° 32 EB, 37°41,

17 km SE ot Millicent on-road to Mi. Gam-

hier, in. sandy soil with grass, bracken and

Drosera, Tringing a Pinus radiata plantation,

TW, 15, viii, 1972—HA (AM).

Remorrs) G, similis belongs io a G. dorsalis

complex including alsa G. ovtothecatus Tt

98 Kh. G M, JAMIESON

differs from beth the faller species in having

only 3 pairs of spenmmuthtecae. Its accessory

genital markings haye the same distribution

as in G. dorsalis, though better developed, but

it differs fram this species in the unpaired fc-

male pore and absence o] seminal vesicles From

LX, in addition to the smaller number of sper-

mathecae and their more ventral location rela-

live to setal lines. Diflerences between the

three Species are minor relative to these be-

tween most other species of the genus but

union of the three entities under G. dorsalis

at present appears unjustified,

Gemascolex stirling) (Fletcher, 1888.)

FIGS 8A, B, 10L. L1G; TABLE 9

Perichacta stirlinu’ Fletcher, 1488a; 395-398;

LSK9b; 1017-1019,

Megascolex stirling? Beddard, 1895: 373,

Michaelsen, 1900: 222. Jamieson, 1971b: Y5,

Fdmonds & Jamieson, 1973: 23-

Meguscelex fletcheri Shannen, 1920; 301-314,

PL XXVII-XXNT, ’

fron| Megaseolex fletcher’ Michaelsen, 1207b-

2t.

Length — 300 mm, w ¢midelitellar) = 12

mm, s — 258 (Specimen |, Specimen 2 is a

posteriar amputee). Pigmented dark olive-

brown dorsally. Circular in cross section, Pros-

tomiunt deeply bisected by a dorsal cunulicula,

epilobous 1/2, closed. but peristomium with

Aumerous longitudinal furrows all round so

that prostomium might be considered epilany-

lobous: transverse Eurrows render peristomium

und prostamium mammilate, First dorsal pare

4/5 with, in specimen 1, an imperforate rudi-

meht at 3/4. Setac well developed ventrally

to midlaterally, rudimentary further dorsally;

aa = ab but sctac progressively more closely

speed dorsally. Numbers of setae per segment

not or only approximately countable, 22 in

XU, 20 fifteen seximents from the caudal end

in specimen J; @ lines straight, z lines irregular,

a Wide ventral and wider dorsal break in the

getul circlet present throughout. Setac a. bd

and c absent in XVII, Few intersctal distances

measurable,

Clitellum XIV—XVI1 (= 4 segments). Male

pores transverse slits with low but tumid Sips,

shortly mediag of setal lines c of NVITL, the

potes §,43=6.71 mm, 0.20-0,21 clrcumference

spurt (specimens {| and 2): each low poro-

phore Iying in a depression and accompanied

laterally by a raised slightly Jargct transverse

ridee: the border of the scgment immediately

in front of and behind the pore also. thickened

10 forin a narrow callosity (specimens 1 and

2) of a small interseymenta) tubercle present

TABLE Ut

fucersetl ittstances in Gemascoles stilingi

standatdived

of cir-

mint cumference

da at u ae ab

Segmeny Nil

Specimen t 20 Le 18.0 cs 43

Socelmen 2 1.9 11 28,0 a6 4,1

Mein Ag 4.7

Interval/xb 16 io

Speeimon XX

Svectmen t 26 12 Av0 73 45

Spectmen 2 i+ 14 55.0 aS a3

Moan 6.9 44

Enteryal/ab 2.1 19

in front ot and hehind each pore ar 17/18

ispeeimen 3). Paired eyelike accessory genital

markings in 16/17, centred in wi nearer ph,

and in 19/20-22/23 (specimens 1-3), those

in 19/20 centred slightly median of «, those

in 22/23 slightly literal of & (specimens | and

2) or those in 19/20-22/ 23 all tn be {speci-

men 3}: the markings with raised whitish cen-

tral ureu,

Paired postsetal oval genital markings with

porclike centres immediately in front of and

wightly Jateral of but contiguous with the sper-

mathew! pores, in VIL VIC and VII (speci-

mens 2 and 3). Spermuthecsl pores 3 pairs, m

6/7. 7/8 and 8/9. lurge pores with wide lips

forming un ellipse, in Lhe Sth to 7th setal line;

the pores, at 8/9, 13,57-14,43 mm, 0.44-0.45

circumference apart (specinien L andl 2),

Strongest septa 9/10-12/13, very thick. Last

hearts in XE. Supra-ocsophayeal 1/72 VUI—

XII, well devefoped, Gizzard in VI. Intes-

tinal Origia XVIT, typhlosole rudimentary, a

slight thickening of the roof of the inlestine

middorsaily, first discernible in XXVIL Neph-

ridia: paired tufts with composite [multiple)

ducts in If, LL, IV and Vo. wll large but in-

creasing in size posteriorly, these in V very

large: the tufts in IV and V open into the

pharynx; the ducts of thase in ILL apparently

join the buceal cavity though some ducts open

at intersegment 1/2: whereas those in 1) appear

wl tu be exonephric in the vicinity of 1/2

{specimens | and 2}. Dense lateral bunds of

numerous {exsonephne?) micromeronephridia

lice in VI-XI on the parictes at the posterior

septum. in XIT-NEX nephridia are anterior as

well as posterior in the seyment, heing

especially dense in MYI-XVE; in XX pos-

teriorly they are anterior only in the segment,

Caudally with numerous large meronephridia

on each side, adherent 10 the posterior faces

of the septa on the intestine and body wall,

each with a large single preseptal funnel which

EARTHWORMS FROM SOUTH AUSIRALIS a

has a long inflated neck, the nephridial ducts

difficult te trace hut apparently (all?) open-

ing into the intestine (specimen 1).

Sperm funnels iridescent in X and X1, Semi-

nal vesicles racemose, in XI and XII; a fur-

ther pair of similar but smaller sacs on the

anterior septum of XIII (specimens 1 and 2)

median to the ovaries (1) or separate uvaries

not developed (2), Ovaries consisting of many

allenuated chains of large oocytes (specimen

1). Large sacs on the anterior septum of XIV

may be ovisacs but show no loculi (specimens

! and 2), Prostates tongue-shaped, lobulated

and. incised, restricted to XVI, the glandu-

lar part passing directly laterally, with slit-like

central lumen the greatest width of which is

only about one tenth the width of the gland,

Lc. gland tubuloracemose; the muscular duct

S-shaped, with an abrupt bursa-like terminal

dilatation. White paired glandular masses in

each of segments XVII, XIX—XXIII, cor-

responding with the external genital markings,

large with the exception of those in XIX

which correspond with the rudimentary mark-

ings in 48/19. Similar paired masses on the

KIV

A Amin

bedy wall in VL VII and VIII in line with

the spermathecal ducts; and corresponding

with the external genital markings. Sperma-

thecae 3 pairs, in Vil, VIII and IX, increasing

in size posteriorly; diverticulum (inseminated)

Single, clavate, unijoculate (specimens | and

2).

Field. variaiion; Specimens {-4 have a circular

genital marking anterolateral to ¢ach sper-

Mathecal pore (with sporadic omissions)

whereas in specimen 5 the marking is postcro-

lateral, in the succeeding segment. Genital

markings at 16/17, at or near 17/18 and. 18/

19, and in 19/20—22/23 are constant in all

specimens and ure paired with the exception

thal that on the Jeft in 22/23 is absent in

specimen 3,

Material examined: Igl, 138°03°E, 32°46’S,

Alligator Gorge National Park, under rocks

near creek in gorge, BJ. and T.F,,

19, vili.1972—specimens 1 and 2. Jg?,

I38°10.E, 32°48'S, Mr Remarkable, under

moss in soil pocket in scree of mountain

side, BJ., 17.viii.i972—specimen 3, Jh1,

Fiz, 7. Genital fields of: 4, Gemtaccolex walkari, holotype, 1k &, G. newmani, Warren Gorge speci-

meq,

138° TSE, 33°035°S, 21 kay from Gladstone

wloug road tw Port Auguslu, in red loam

jiimong red voms hy road, HI and TOV.

1S.¥lii,1972—specimen 4. Ji2, 138°42’E.

35°0S, Craters, meur Adelahle, R.A,

24.51.197l—specimen 5, Specimen ] (BM),

specimen 3 {AM)\ specimen 2 (SAM);

specimen 4 and 5S (BJ).

Remarks: Location of tbe genital markings in

16/17 median to Une mule pores, while those

in 17/(8-221/23 ure approximately in line with

these pores, permis ready identification of G.

valeting,

Seumascolex walkeri sp. nov.

FIGS 7A, 10M, 11H; TABLE 10

Length = 42 mm, w (midclitellat), = 3

mm, s = 107, 1LI(H. Pl). Pigmentless in

aleohol, Circular in cross section, Prostomium

epitanylobous, posteriorly convergent, narrow.

First dorsal pore 4/5. Sclue a& and he wide

throughout and approximately cqual, being

slightly wider than other intersetal distances of

a side antenur to the clitellum; posterior to

the clitellum ab and Se remain the largest in-

tervals bur spacing of other setae becomes very

irregular, Numbers of setac per segment 14 1A

NI anc XX (H, P1), 18(P1)-22(H} filtcen

segments from the caudal end; a lines straight

throughout: z lines straight in the forcbody,

irregular in the hindbody; a moderatcly wide

ventral break visible throughout; a dorsal break

clixcernible in the forebody but not present in

the hindbody. Setag a and & absent in XVII.

Clitellum rudimentary, some annwar modi-

fication un XIV-XVI. Male pores on hemis-

pheroidal parophores in XVII: the pores

2.29¢P1)—278(H) mm, 0.30(P1)—0.34(H)

circumference apart. Paired cyclike ventrally

conjoined yvenital markings in intersegments

17/1K-24/ 25. converging posteriorly from ab

in 17/18 to @ in 24/25 (H, see Field Varia-

tion}. Spermathecal pores L pait, ventral in

5/f, small elliptical papillae in setal lines ¢y

2.49(H)—2.64(P1) mm, 0.34(P)}-0.38 cir-

cumference, apart. Sirangest septa 10/11 und

11/12, moderately strong. Last hearts in

XIIl, Supra-oesophageal traced In IX-XUE.

Giezard in V. Intestinal origin XVIT; a deep

laminar dorsal typhlosole commencing in XXI

Or XXIP but continuous ag a rudiment forward

into XVII, Nephridia: Paired meronephrie

cufts in ff. EIT. TV and V with composite ducts

opening into the pharynx; very large in V_ de-

creasing in size anteriad (H, PL), Traneverse

hands of nmumerous astomale. micromero-

H, Gi, M. JAMTESON

TABLE 10

lmersetal slistances in Gertmiscolex, wilkeri

siandarived as 6

mm af crcamterenee

. aa ab my 22 o aa ab «your

Seement X11

Holotype 1.2 OF Wo U7 7.2 1s 28 79 84

Paraiyne 1 06 OF US DE FH IF TO Gt WT

can 056 74% 65 99

dnterval/ah 1.4 40 10 th

Sremea, FOS

Holnuyre 08 07 6.7 06 60 01) Sa af 79

Paratype 1 08 OF OF Ba 7.9 $2 WG 74 98

Mean TOU Ra FR Re

Interval/ab T2 TU TY 10

nepheidia exonephric on the body wall in VI-

VIM associated ity IX—XV with the posteriur

septa. ig XVE with the anterior and posterior

sepla, and in XVIE and succeeding segments

with the anterion septa: all septal oephridia

lacking detectable parietal ducts (entero-

nephric?) (H), Coudally, from abouwl segment

70, with fewer, larger nephridia, approximately

5 on wach side, exch with a preseptal turinel,

the nephridial ducts running on the posterior

face of the septum fo join the ventrolateral

wall of the intestine, some suggestion of u

longitudinal duct joining those of adjavent seg-

Ments seen on the side of the gut hut requiring

confirmation; postseptal nephrostomes absent:

some oustomate, parietal anil apparently

exonephric micromeronephridia present in

caudal segments in addition to the stomate

nephridia (HA, Pl). Sperm funnels weakly

ifiulescen) In X and XI: seminal vesicles race-

mose, almost sacciform, in XI and XI.

Ovaries bushy with several stcings of Jarge

oocytes: smull sues in NTV may be ovisaes.

Prostates Mattened, leaflike, with deeply in-

ciscd murgins and a grouvelike ‘midrib’, re-

stricted to XVITT; duct U-shaped, bent median-

wards, the ectul limb preatly thiekened: vas

defetens joining the ental limb. at midiength,

Spermuthecue one pair, in VIL divertictuluim

(uninsemingted) single, digitiform, unilacu-

late, slightly longer than the ampulla {H, Pt).

Wield variations In the sexual, though imper-

fectly clitellate types (holotype and 4 para-

types). genital markings are consistently

present in the seven inlersegments 17/18—

23/24 but those tn 20/21—23/24 may be spor-

adically absent unilaterally, Only Pl agrees

with the holotype in having a marking (uni-

lateral, night) in 24/25.

Miyerial examined: Jil, J38°38°E, 35°00°S,

Belair National Park, dry geass ant eucalypt

selerophyll, T.W., 2Lvii1972—H, PIl-4

Jiz, ('38°42'E, 34°S8'S,) Mi Lofly, in

eucalypt woodland, BJ, and = T\W,,

EARTHWORMS FROM SOUTH AUSTRALIA 101

XIV

Fig. 8 Gemascoles stirlingi, Genital fields of: A, specimen 1, Jgi. B, specimen 3, Jg2.

16.vili.1972—P5 and 6. H, P2 (AM); Pt,

P3 (BM); P4 (SAM): P5 and 6 (BJ).

Remarks. ‘The single pair of spermathecae,

resiricted to VI, distinguishes this species.

Genus SPENCERIELLA Michaelsen, 1907a

emend.

Terrestrial, Body circulat in cross section.

Prostomium epilobous; peristomium usually

bisected by a Jongitudinal furrow ventrally

which is more conspicuous than other grooving

which may be present. First dorsal pore 4/5

or 3/6. Selac numerous in each segment. A

pair of combined male and prostatic pores on

XVITI. Clitellum annular, anterior to 17/18.

its intersegments and dorsal pores obscured at

maturity bot setae. visible. Segmental accessory

genital markings present. Female pores paired,

in XIV, anteromedian of setue a. Spermathecal

pores in 2-5 intersegments ending in 8/9, or

a pair in 7/8 only; single or paired.

Dorsal blood vessel single, continuous onto

the pharynx, Last hearts in XII or XIII. those

in X posteriorly latero-ocsophageal, each aris-

Ind

ing from the short supra-cesophageal vessel

and From the dorsal vessel. Subneural vessel

absent. Gizzard large, in V. Three ar four pairs

of well-defined extramural glands, typically

with many internal septa, dorsoluteral on the

oesophagus, in X, XI-XILL Typically with a

latera-oesophageal vessel on each side supply-

ing the caltiferous xlands. Intestine commenc-

ing we XV or XVI of (8, hall’) XVI) typhlo-

sole 2 low dorsal ridge or absent; cacca and

museulir Ubickening ubsent, Excretory system

meronephric. Fharyngeal tufts present an-

leriorly, succeeding segments with astamate,

exnnephric — mecromeronephridia, Caudally

(always?) with several nephrostomes on each

side in each segment or with all but the

median-most funnel reduced; with (always?)

some at least of the meronephridia entero-

nephric nil interconnected hy a longitudinal

paired excretory duct f{ureter). Testes and

funnels in X and XI; testis-sacs absent: semi-

nal vesicles in 1X and NIT,

Ovaries and funnels in XL]; ovisacs present.

Prastates rubuloracemose (partly or wholly

linear with central lumen) or racemose (here

bipartite}; vasa deferentia joining their mus-

culur ducts near the glands, Spermathecae each

with one or more clavate, uniloculate diver-

liculit,

Type-species> Diporechaeta notabiliy Spencer,

191)

Distribilions Souch Austratia,

“Tasmaniin, New Zealind?

Vietona and

Creckiisr or Srecits

* New eouthinations in Spercericlte,

South Australis:

|, Spevicepielle impuricysis sp. nov.

1, Spenceriella peitolacasis sp, nuy

Vietor:

Perichaeta freachl® Spencer, 892

Periehaeta halli* Spencer, 1892

Perichaeta hogei* Spencer, 1892

Niparachaeta notabilis Spencer, 1900

Perichaeta rabra® Spencer, 1892

Perichaeta steeli® Spencer, 1892

Perichaeta sylvatica* Spencer, 1592

’

CON DAR

Tasmitnia:

10. Perichaeta tasmanica* Spencer, 1895

Species incertae sedis:

11_ Megascolex antarctica Baird, 1871

svn, Diperochacia shakespear’ Benham,

1906 (New Zealand)

B. G. M. JAMEESON

12. Spenceriella argillne Lee, 59 (New Zea-

land)

13. Diparechaeta gigarledn

(New Zealand)

14, Diperochaeta miplestent Spencer, 1900

(Vicloriz)

15. Spenceriella pallida Lee, 1959 (New Zea-

land)

Remarks: Jamieson (972) described 2 neo-

typic specimen of the type-species, Spencerielle

norrhilis. The specimen was in very poor con-

dition and it was only possible to say of the

several rows of meronephridia that a presep-

tal funnel was seen in one segment an the

nephridium nearest the nerve cord. This sug-

gested membership. in the tribe Dichogasirini.

a group characterized by a single preseptul

funnel on the medianmost nephridium on each

side in caudal segments. Three other species,

of which material has been examined by the

author, are clearly cangeneric with Spencericlu

notahtliy trom their general morpholegy and

particularly from, the form and urnimwement of

extramural calcifernus glands, These are the

two new species 5. fiaparieystiy and S$. peno-

lueusix anct a species provisionally placed in

Megascolex by Jamieson, 1974. Perichaetya tas

manica Spencer. 1895, The two South Austra-

lian species have multiple caudal nephrostomes

with enteronephry and therefare show that

Sperceriella must be consigned to the tibe

Meeascolecini. Only the median funnel on each

side was identified with certainty In the new

material of P. rasmatien bul what appeurcd

10 be vestivial funnels were present laterally to

this and caudal enteronepbry was demonstra-

ted for the median nephridium. This suggests

4 sceondary approach to the dichogastrin con-

dition Tn this species The other species in-

cloded phove in Spenceriella agree closely with

the three studied in generu) morphology, in-

clading the arrangement of calciferous plands,

though details of excretory and vaseviar sys-

lems are unknown. Occurrence in one and the

same genus of linear lobuloracemose or bipar-

tite prostates with branched ducts, further con-

firms the author's contention (Jamieson

1971a) that the form of prostate glands has

only very secondary importance in the ctasai-

fication of megascolecids, contrary to the view

of Gates (1959),

Other species included by former workers

in Spenceriella are listed by Jamieson (1972:

73). OF these Perichaeta lateralis, tentatively

instuded by Michaelsen 19074, ig bere placed

in Gemescolex, The remaining species pre-

Benham, 1906

EARTHWORMS FROM SOUTH AUSTRAIIA

viously included are ireated above as incerrae

sedis because, though not placeable in Spen-

cerielly a5 homogeneously defined above, they

are nor uf present placeable elsewhere without

premature erection of new genera for their

reception. Megascolex uaturctice placed. us

Diporachaeta shakespeari, in Spenceriella by

Michaelsen (19074) deserves separate com-

ment, From its, albeit inadequate descriptions

this conforms sufficiently closely with the

ibove generiv definition Cineluding calciferous

glands in XJ-XEf1) 40 ¢onceivably be con-

generic with Spetceriella norahilis bue little is

known of its nephridia hevond the existence of

hands of meronephridia. Its peregrine distribu-

liom in New Zealand wnd its islands rakes an

Austealian origin uf this species or an ancestor

conceivable.

Spenccriclla imiparicystis sp, nov.

FIGS YA, LON; TABLE 11

Length = 44(H)-45(F1) mm, wo (mid-

clitellar} — 2.8 mm, s = 1U7(P1}-122(Hb.

Pizmentless in alcohol Prostomium mot cana-

liculate, epilobous 1/2(H)-2/3(P1) open but

with two weak transverse furrows anterior 10

ils posterior limit. First dorsal pore 4/5, but

an imperferale rudiment at 3/4. Setae subs

equally spaced: 24 in XIL, 22(H)-23(P1) in

XX, 22 caudally: @ lines straight, z lines irregu-

Jar; a ventral break appreciable throughout; a

Jorsal break present only in seme anterior

segments. Setae a und A ubsent in XVII

Clitelum weakly developed, 1/2 XITI-XVII

(4 1/2 seements), dorsal pores, intersegments

and selac retained (H=: not developed in Pl).

Male pores quadriridiate apertures jn ab of

XVITL cach atthe centre of an oval papilla in

aw Very strongly protuberant paired porophore

which fills the segment longitudinally and ts

wider than long; cach porophore almast tauch-

ina the other; the pores 0.77 (P1)-G.88 mm

(Hy, 0.1 circumferences apart. Accessory geni-

tal markings paired midventrally conjoined

lumescences filling their scements fongitudin-

ally and With presetal pore-like centres

luteral of & in XL and In «bh in XVII

amd XIX. A pair of small elandular areas

present posteriorly in cach of VIT and VIEL on

each side of the spermathecal pore af the sev-

ment, On a imidventral elliptical tumescence

sitaddling 7/8 and 8/9 (H, Pl; see Field

Vitiation). Spermathecal pores unpaired, mid-

ventral, in 7/8 sod 8/9, ench continued an-

teriorly as a short slit bisecting the posterior

part of the surrownding tumescence.

1D3

TABLE 11

Hiteesetal distances in Spenceriella imparicyslis

Se ee

Stundardiz=d s3%

ini oF clroumfenenoe

ab aw or u a 2 Ww 2

Sequeent XTL

Hotere O7 OS O63 O4 78 O95 38 42 SD

Paratype 07 02 OF OF Te OS Bl 48 4

Mean “5 33 40 42

Tilerval/ab 29 10 12 146

Seement XX

Holoiyee 07 07 O02 O02 99 70 25 20 35

Patatype | O6 027 03 83 Ba 79°29 24 Ft

Mean 7A 77 UT DB

Tntetyal/ab 77 10 Im to

Stronvest septa 9/10-11/12, inoderately

sirong. List hearts in XII} those in) X—XIL

latero-oesophageal, each originating from a

transverse vessel (calciferaus vessel) which

bounds, and tamifies over the correspowding

caleiferous gland and receiving (observation

from one heart) at its junction wilh this vessel,

a slender connective fromr the dorsal blood

vessel} a continuous supra-cesophageal vessel

not demonstrable; the two calciferous vessels

on each side in a segment join in the midling

helow the dorsal vessel, al the doreal

extremities of the glands high above the

acsophagus. Cammissurals in VII=IX well de-

veloped but dorsoventral only and, unlike the

latcro-vesophageal hearts, giving ventrally

branches to the parietes. A lavero-oesophageal

vessel present on each side median to the

hearts, thickest in Eront of the calciferous

giunds to each of which it contributes a branch,

becoming suboesuphageal and subpharyngeal

in front of the gizzard.

Gizzard farge, with anterior rin, firmly mus-

cular in V. extending posteriorly to interseg-

ment 10°11; free oesophagus in [TV not as wide

as the gizzard, Oesophagus only slightly shorter

in VE than Llutiher posteriorly: conspicuousiy

vascularized, moniliform het fairly narrow in

VITT and IX; in each of X, XT, XM and XU

hearing a pair of ovoid vertically elongated

true calciferous glands, the short narrow stalks

of which join the dorsolateral wall of the ueso-

phagus, the glands lying above the oesophagus

and cach contiguous with its partner

medianly; each gland with numerous Jamellac

projecting from the walls and grouped radially

around the long (vertical) ais of the sinnd,

almost contiguous axially but no union demon-

strated; each gland, with the exception of the

pair in XII, circumscribed on ites outer side

hy the corresponding heart, Intestinal origin

XVI; a very low, Indefinite dorsal ridge com-

Mencing in XVII. scareely justifving recog-

nition as a typhlosole; muscular thickening and

Fig.

caecca absent. Nephridia: a pair of very large

tufts with innumerable spiral loops in V sends

composile ducts anteriorly to join the wall of

the anterior region of the pharynx (entero-

nephric): much smaller tufts in [VY are not cer-

tainly cxonephric; while aggregations of

nephridial tubules in I and IJ! are exonephric,

via sheaves of ducts, at the anterior margins

of their respective segments. In the anterior

intestinal region with numerous parietal asto~

B. G. M. JAMIESON

9, Genital fields of: 4. Spenceriella imparicystis, holotype, L-k4. B, 8. penolaensis holotype, Lm1.

mate, exonephric, micromeronephridia. Caud-

ally with several enlarged nephridia on each

side, each with a singie (presceplal?) funnel.

Lateral nephridia exonephric; more median

nephridia contributing their ducts to 4 common

iransverse medianly directed duct which joins

the dorsal surface of the intestine shortly

lateral of the dorsal blood vessel; a longitud-

inal duct which apparently connects these seg-

mental nephridial ducts visible running through

EARTHWORMS FROM SOUTH AUSTKATIA

some caudal segments (H, P]). Sperm funnels

iridescent in X and XI. Ovaries slender, pin-

nate, with large gocyles, True ovisacs contain-

ing oocytes in XLV. Prostates with 4 flattened

laterally directed tongue like portion in XVII

which t juined at approximately mid length

by a tortuous, depressed almost tubular por-

hon in XIX, the entire gland not linear but

having the appearance of derivation {rom a tor-

tuous depressed tubular gland in which some

adjacent adpreszed coils have united; vas

deferens joining the steaight muscular duct

Where this joins the gland. Spermathecae un-

paired, midveotral, in VINE and EX: each with

2 (inseminated?) clavate uniloculate diver-

ticula, the two diverticula projecting of both

sides of the ventral nerve cord and (ne of them

passing under it to join the wide spermathecal

duct where this enters the body wall (H, PL).

Field variation: In the four type-specimens the

accessory genital fields are constant, with the

exception that thé paired markings in X are

absent in paratype 2, probably owing to im-

maturity, Two immature specimens, not desig-

nated types, from locality LIZ have genital

fields and an internal anatomy which suggests

they belong to this species but all genital mark-

ings are slightly more median than in the types.

The median markings at 7/8 and 8/9 are

absent bit spermathecae are unpaired mid~

yentral at 7/8 and 8/9, the paired segmental

markings in X have centres presetal in ab:

those in XVII are absent but there is a pair in

each of XIX and XX presctally and slightly

median of a; the male pores are median to a

lines.

Mudlerial examined: ka, 140°44'E, 36°59'S,

1.6 km § of Naracoorte, in sandy soil with

bracken and wattles near pasture, BJ. and

T.W., 16.40. 1972—H, Pi-3. LI2, 16 km

SE of Millicent en road to Mount Gambler.

in black soil Under mallee gums, BJ, and

TM V5 viii.1972—2 semi-mature specimens

not designated types. H (AM): P1—2 (BM);

P3 and LI2 (BI)-

Remurks: Spencerigila onpurievstis is mor-

Phologically very similar to the type-spectes 5.

naiabilis (see Jamieson 1972). the genitul

fields in the specimens from locality LI2 being

especially similar. The similarity extends to

locatton of jatero-oesophageal hearts in X-XIE

with calciferous glands in X—XIIM. The un-

paired spermatheexe in VIII and TX in S§,

imparicystis clearly distinguish it from § nora-

hilis which has a pair ot spermathecae in VIL

only, The paired spermathecal diverticula ate

alsa distinctive, The distribution of calciferous

glands and hearts distinguishes |t, among other

features, from §, penolaersis,

Spenceriella penolaensis sp, 1,

FIGS 9B, 10 0; TABLE 12

Length — 43-54 mm, w ¢(midelitellar) —

3 mm, s = 79-128 (H, postenur amputee?,

Pi). Pigmentless in alcohol, Prostomium

canaliculate, epilobous 1/2, with transverse

furrow at 1/4, the lateral grooves. continying

almost to intersegment 1/2. Dorsal pores very

large, the first at 4/5. Setac small and dificult

to discern, subequally spaced but he signifi-

cantly wider (hat wh; a@ lines straight, z lines

regular; a ventral break well developed

throughout, a dorsal brenk present except in

some caudal segments. Intersetal distances in

XX not measurable. Setaec a and / absent in

XVIUL

Chitellum XUM-XVIUL, but in XVI present

only dorsal to the genital murkings. Male pores

in ab of XVII, each a small orifice on an

approximately hemispheroidal porophore

which is laterally skirted by a tumid ridge: the

pores 0.56(P1J-O.88(H) mm, 0,05(P1)-0.12(H)

circumference apart but not accurately

measurable as body wall ts depressed betweert

pores. Accessory genital markings all scgmen-

lal. not intersegmental; a pair of large tumid

whitish pads filling their segments long-

itudinally, each with central circular area dis-

tinct from a peripheral strongly \umid rim, ex-

tending laterally of ¢ lines in X und XT. with

centres stighily postsetal and lateral of & (H,

Pt), and in XVI (right only) (H). XVII,

XIX, XX (H, PL) and XXU (paired) (H),

with centres slightly presetal and Jateral of 4;

most genital markings medianly conjoined (see

Ficld Variation), Spermathecal pores 5 pairs,

in 4/5-8/9, in & lines: scarcely tecopnizable

extemally| the pores 1.47 mm (H, P1),

O.15(P1)-0.16(H) circumference apart

Strongest septa 9/10-11/12, moderately

strong. Last hearts in XtIL, those im X—NTH,

each arising from a supra-nesophageal vessc)

{in XJ or from a transverse vessel bounding

TABLE 12

interseta? distances ta Spencericlla penolaensia

Slandetdired as

nin Of étreumferenze

yee u ax oat ouy 22

Suement X11

olowne 0.6

Paratyre 1 0.7

Mean

{nterval/ab

the corresponding calviferous gland (ta XI-

NIM) and receiving a long slender connective

fram the dursal blaod vessel; otherwise Un-

hratiched, Comrmissurals of VE-LX dorsoven-

irat only, slender though, like the posterior

hearts. valvulun but differing from the latter in

ventrally yiving branches tu the parictes,

Supra-cesophigenl vessel not demonstrable as

a cormtinvous vessel but seen in X and XTIL

Gizzard very large, ovoid bor fattened at

the anterior wider end, firmly muscular in V,

(septum 5/6 exceedingly attenuated) its

posterior end extending almost to inlerseazment

10/11, Oesophagus very shore in VI-X hut m

each of XI, XIf and XI bearing a pair of

ovoid vertically clongated tric calcifernus

glands, the shore narrow stalks of which join

the dorsolateral wall of the oesophagus, the

glands lying above the oesophagus and each

contiguous with its partner medianly; cach

gland with numerous lamellae projecting fram

the walls and grouped radially astound the long

{yertical) axis of the gland, scveral uniting

axially. the others almast contiguous but not

liniting; euch gland circumscribed on its Outer

side by the corresponUing heart. Intestinal

origin XVI; a low irregular dorsal typhlosole

commencing in XX caeca and muscular

thickening ubsent. Nephridia: astomate mero-

nephridia in TL loosely aggregated into tufts

send sheaves of ducts dorsolacerally to inter-

segment 1/2) similar aggregations in II-V¥

also appear to be exonephric. are adherent ta

the pharynx and are apparently ut least partly

enteronephric, what appear to be pharyngeal

iluets. being demonstrable in PI. Succeeding

ocsophageal and intestinal segments have each

4 lransverse row of approximately LO ustomace

parietal micrameronephndia on each side.

Cuudally (Pt and 2) with several somal

nephrnstomes (one to a meronephridium) on

euch side in cach segment, each Funnel lying

in the segment projecting from its mephridial

body near its duct and not preseptal with the

exception of the medianmost nephridium

which, in some segments was seen ta have i

preseptal funnel, At leasl some of the neph-

ridial ducts in each segment combine to send

a duct to the dorsolateral surface of the intes-

tine; these ducts communicating from segment

to segment by a longitudinal wuct on each side

which runs on the external surface of the intes-

tine of several segments where visible but is

nol demonstrable, and is therefore questian-

abte continous, throughout the cauda) region.

Confirmation of the exact arrangement of the

B, G, M- JAMIESON

nephridia of this species is required as unusual

difficulty in demonstrating the structures des-

scribed precludes certainty that the pharyngeal

and all caudal nephridia are emeronephne and

acttial openings of the caudal ducts into the

intestinal lumen have not been demonstrated.

Sperm Funnels iridescent in X and XJ. Ovaries

bushy with many chains of very large oocytes

(H, P1); ovisacs absent (H) or well developed,

containing numerous oocytes, on the antenor

septum of XIV (Pl). Prostates tubulorace-

mose. bobulated but linear, the gland folded

once and occupying XVII and XIX, with very

nurrow central lumen throughout, surrounded

hy thick vlandular walls; the curved muscular

duct joined near its junction with the gland by

ihe vas deferens. Penial setae, and internal

glands corresponding with the accessory peni-

tal murkings, absent. Spermathecae 5 pais,

diverticulum (inseminated) single. clavate,

uniloculate,

Wield variaion: In the eleven typeespeciinens,

including the holotype, paired genital markings

with centres lateral to 4 and slightly postsetal

are invariably present In X and XI; paired

genital markings with centres lateral to 6 and

slightly presetal are invariably present in XVIT

and XIX, occur in 6 specimens in XX (FH,

P1-3, 6, 10), and are represented, on the right

only, in 2 specimens 1H. PO). Female pores

are always paired, presetal, 1/3-L/2 az apart

aud spermulhecal pores are never discernible

with certainty externally.

Material examined? LI, 140°49°B, 37°28'S,

11 km S of Penola. in cucalypts (ringing

Prius radia, BJ, and TW. 1S.vdi.1992—

P7-I0, Lml, 140°S5°E, 38°OL'S, 26 km

from Mr. Gambier along roud to Nelson, tn

sundy loam under grass among wattles end

sums with some herbaceous garden escapes.

AJ, and TW, WSwliil972—M, PI,

H. P2-4+ (AM): Pl, 5, 6 (BM}) P7-3

(SAM); P9, 10 (BI).

Remarks: S. penolaensis is distinguished fram

the type-species, S$, nelabilis, and from 5, Im-

parieysris, ty having only three pairs of cal-

ciferous glands, lacking those of X_ It dilfers

fram hoth species in having five pairs of

spermathecae and in other respects,

Discussion

The earthworm fauna of South Australia is

remarkably impoverished, though of high

specific endemicity. Tt has been shown above

that the teral known fama in the only

Indigenous family, the Megascolecidae, con-

EARTHWORMS FROM SOUTH AUSTRALIA 107

——— iim ———

Fig. 10, Spermathecae (right segment 1X unless otherwise imdicated): A, Perionychella (P.) incan-

stans, holotype, Hil. 8, Hetéroporodrilus shephardi armatus, LI. C, Gemascolex bursatus,

holotype, 3j3. D-F, Gemascelex lateralis; D, specimen 1, Ji2; E & F, specimen 3, LIL (dorsal

and ventral views, right VIII). G, Gemascolex mirabilis, holotype, Jg2. H & 1, Gemascolex

octothecatus; H, holotype, Lml; /, paratype LU. J. & K, Gemascolex similis; holotype, L12

(J, left WI; K, left IX). L, Gemascolex stirlingi, specimen 1, Igi (left IX). M, Gemascolex

walkeri, holotype, Jil (right VI). N, Spenceriella imparicystis, holotype, Lk4 (unpaired, IX)-

O, Spenceriella penolaensis, holotype, Lm1.

sists. of A peregrine species of Micrescalex, a

single species questionably assignable ta

Perionychetla (from Kangaroo Island}, 9 3ub-

species of a Victorian species of Helereporo-

drifus, eight species of Gemasceler and twa

species of Spenceriella: m all, ignoring the

peregrine Microscolex, four genera with twelve

species in contrast with thirteen genera with

seventy eight species in neighbouring Victoria

and (welve genera with forly eight specics to

jhe small istanid state of Tasmania. All of its

genera and two species are shared with Vic-

foria, South Australia therefore has close

zoogeographic affinities with Eustern Ausiralia.

Apart fram the fact that the Kangaroo Island

Pertonychella shows aflinities with the genus

Grefiophilus in’ Western Australia, there are

Ho generic or specific affinities with the latter

stale,

The paucity of the fauna of South Australia

is correlated with its low rainfall. A south-

eustern coustal wedge, the Fleurieu und Yorke

Peninsulas anu Kangaroo Island are the wettest

parts, with an annual rainfall, with local excep-

Hons, of between 500-750 mm (20-30 inches)

but the remaining coastal region, including the

Evre Peninsula, has only 400-500 mm [16—

20 inches) or very much less and the interior

is virtually desert. Pickford (1937) in a very

thorough survey of the earthworm fauna of

South Africa found no earthworms whete the

rainfall was less than 25 inches and the wetter

parts of South Australia are near, often below,

this limit, The rainfall in coastal Victoria, in

contrast) varies from 500-750 mm (20-30

inches) in the drier west to 750-1975 mm

(30-80 inches) in the eas! while Tasmania

&.G. M JAMIESON

also has areas ranging from 500-2000 nim but

is generally wetter than Victoria,

Of the regions in South Australia not investi-

gated ior earthworms. only the Yorke Penin-

sula appears to be wet enough to yielul earth-

worms and though some additional species

doubtless remain to be discovered in the areas

from which they have been collected, if is

unlikely that further collecting will elevate the

South Australian Fauna above a total of about

twenty species.

it ts noteworthy that the great majorly of

South Australian species, all in Genurcolex

and Spenceriella, have caudal enteronephry, a

cenditien which would appear to be an ulup-

tation for water conseTvation 28 urine exercted

into the intestine is presumably concentrated

by resorption of water in the hind gut, The

close similaricy of the species within Geinay-

colex, as im Spenceriella, suggests relatively

recen( speciation from aii-even smaller fauna,

Acknowledgements

The author is indebted to Mr. G. Gross of

ihe South Australian Museum for the loan

of material and to. Mr, Ifor Thomas and, Dr.

S. Edmonds for donation of specimens. Mr. T,

Walker is thanked for his indispensable aid in

the field and for uxsistance in mapping and

other respects. Thanks ate also duc to the

Electron Microscope Department, University

of Queensland for printing the micrographs

of setae, A illustrations are by the author.

The work was made possible by Australian

Rescarch Committee grant no. 239260-R-Zool-

ARGC-120-72 and by a Royal Society Nofficld

Bursary,

References

Barsp, W. (1871)—Megascolet aeteretien, an

earthworm from New Zeulund. Proc. Linn.

Soc, Lond, 11, 96.

Bentham, W. RB. (1906).—Farthwarmys fram Lie

Barrier fsladd. Trans, NZ, Inst. SB, 248.256.

Boanoman, W. (1943)—On a collection of Oligo-

chaeta from the Jenolan Caves District, New

South Wales, Rec. Aust. Mes. 21(3), 148-

17R-

Epsionps, S, J, & Jamieson, B. G, M. 119731.—

A new venus and species of earthworm

(Megascolecidae> Oligachaeta}) from South

fueare. Trans, R, Sad, §. Aust, 97(1), 23-

Frercuer, J, J. ( F8S8day—Notes on Austrulion

eurthworms, Pact U1, Prec, Linn Sac. Wo

2 (ser, 2), 1887, 375-402.

Fraicuen Fo J. (1888b).-—Notes ou Australias

carthworms, Part IV. Proc “ion. Sac.

NS. 2 (ser. 2), 1887, 601-620,

Firrener, J, I (1889a)—Notes on Australian

eurthiweortis. Pact V, Proc. Lili. Sov. NSW.

3 (ser. 2). 1888, 1521-1558,

FiercnerR, J, J. (1889b).—Notes on Austrian

earthworms. Part Vi. Proc. Linn, Spe,

NS Wd (ser. 2), 1889, 987-1019.

Gares, G. FE. (1959) —On a taxonomic puzzle

and the classifiention of the earthworms.

Bull. Mus. comp. Zool, Harv, W214, 229-24)-

Gaves, G. EF. (4962).—On an exotic carthworm

now domiciled jn Louisiana. Prac Lovisittne

Acad. Sci. 25, 7-15.

Tamurson, B, G, M, (1970).—A revision of the

Australian carthworm genus #aadwardiella

with descriptions of iwo new genera, J, Arvel,

Lond, 162, 99-144

EARTHWORMS FROM SOUTH AUSTRALIA 109

Jamieson, B. G. M. (1971la).—A review of the

megascolecoid earthworm genera (Oligo-

chaeta) of Australia. Part I—Reclassification

and checklist of the megascolecoid genera of

the world. Proc. R. Soc. Od 82(6), 75-86.

Jamieson. B. G. M. (1971b).—A review of the

megascolecoid earthworm genera (Oligo-

chaeta) of Australia. Part I]—The sub-

family Megascolecinae. Mem. Od Mus. 16(1),

69-102.

Jamieson, B. G. M. (1972).—The Australian

earthworm genus Spenceriella and descrip-

tion of two new genera (Megascolecidae:

Oligochaeta). Mem. nat. Mus, Vic. 33, 73-88.

Jamieson, B. G. M. (1974).—The indigenous

earthworms (Oligochaeta: Megascolecidae)

of Tasmania. Bull. Br. Mus. nat. Hist. 26.

203-328.

K, FE, (1959).—The earthworm fauna of

New Zealand. Ball. N.Z, Dep. scient. ind,

Res. 130, 1-486.

MICHAELSEN, W. (1900).—“Das Tierreich”, 70,

Vermes. Oligochaeta (Friedliinder: Berlin.)

MicHagBisen, W. (1907a).—Oligochaeta. In “Die

Fauna Siidwest-Australiens” 1(2), 117-232.

(Fischer: Jena.)

MICHAELSEN, W. (1907b).—Oligochaeten von

Australien, Abh. Geh, Naturwiss.. Hamburg

19(1). 3-25,

LER.

PickForb, G. E. (1973),—*A monograph of the

Acanthodriline earthworms of South Africa.”

(Cambridge. )

Rosa, D. (1887).—Sui generi Pontodriluy, Micro-

scolex et Photodrilus. Boll. Musei Zool. Anat.

comp, R. Univ. Torine 3(39), 40.

Rosa, D, (1890).—Terricoli Argentini raccolti

dal Dott. Carlo Spegazzini. Annali Mus. civ.

Stor. nat, Giacomo Doria 29, 509-521,

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

new species of earthworm from South Aus-

tralia, Megascolex fletcheri. Proc. R. Soc.

Viet. 32 (n.s.) (2), 302-313.

Spencer, W. B, (1892).—Preliminary notice of

Victorian earthworms. Part II. The genus

Perichaeta, Proc. R. Soc. Vict. 5, \-26,

Spencer, W. B. (1895).—Preliminary notes on

Tasmanian earthworms, Proc. R. Soc. Vict. 1.

33-54.

Spencer, W. B. (1900).—Further descriptions

of Australian earthworms. part JI. Proc. R.

Noe, Vict. 13 (n.s.) (1), 29-67.

STEPHENSON, J. (1930).—*The Oligochaeta.” (Ox-

ford.)

STEPHENSON, J. (1933).—Oligochaeta from Aus-

tralia, North Carolina, and other parts of the

world. Proc. zool. Soc. Lond. 1932, 899-941,

110 B. G. M. JAMIESON

Prostates of: A, Heteroporodrilus shephardi armatus, paratype 3, Lk4. B-E, Gemascolex bur-

saius, holotype, J)3: B, dorsal; C, ventral; D & E, prostates in sita, Showing bursae, muscu-

lar ducts, and glands adherent to the intestine. F, Gemascolex lateralis, specimen 3, Ll. G,

Gemascolex stirlingi, specimen 1, Jgl. H, Gemascolex walkeri, holotype, Jil. Scale 1 mm.

Fig. 11.

Fig.

12.

EARTHWORMS FROM SOUTH AUSTRALIA 11]

1oum F 104m

—

Penial setae of Microscolex dubius, by scanning electron microscope. A, entire seta with

muscle adherent basally; B, tip of same seta: C, D, E. sculpturing of same; F’, seta of second

specimen, Ll4.

8. G. M. JAMIESON

Penial setae of Heteroporodrilus shephardi armatus, by scanning electron micro: F

holotype, LIl; A, tip of seta; B & C, sculpturing; D, sculpturing of second seta; EF & F’, para-

type 1, Lk4; &, tip: F, sculpturing.

VOL. 98, PART 3 31 AUGUST, 1974

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Rogers, R. W. Lichens from the T. G. B. Osborn Vegetation Reserve at Koona-

more in Arid South Australia - - - - - - 113

Dulhunty, J. A. Salt Crust Distribution and Lake Bed Conditions in Southern

Areas of Lake Eyre North - - - - - - - 125

Mawson, Patricia M. The Genus Potorostrongylus Johnston and Mawson (Nema-

toda: Trichonematidae) from Macropod Marsupials - = - 135

Bourne, Jennifer A., Twidale, C. R., & Smith, Dianne M. The Corrobinnie

Depression, Eyre Peninsula, South Australia - - - - 139

Firman, J. B. Structural Lineaments in South Australia - - - - - 153

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

LICHENS FROM THE T. G. B. OSBORN VEGETATION RESERVE AT

KOONAMORE IN ARID SOUTH AUSTRALIA

BY R. W. ROGERS*

Summary

ROGERS, R. W. (1974) .-Lichens from the T. G. B. Osborn Vegetation Reserve at Koonamore in

arid South Australia. Trans. R. Soc. S. Aust. 98 (3), 113-123, 31 August, 1974.

The Koonamore Vegetation Reserve has a lichen flora of at least 38 species. The level of endemism

(19% confined to Australian arid regions) is lower than that in other arid lands, but the total number

of species is similar to that found in the arid lands of Asia and North Africa, and the percentage of

foliose species is higher. It is possible that either the environment at Koonamore is less harsh than

other areas with similar rainfall, or that Australian foliose species are more drought resistant than

those from other areas. However, the broad species concept followed here, and the topography of

the reserve also, tend to limit the number of crustose species. All soil-surface species occur more

frequently on loamy soils than on sandy soils. It is suggested that Collema coccophorus,

Dermatocarpon lachneum, Endocarpon pusillum and Heppia lutosa, the species most common on

sand and most commonly occurring alone, are the pioneer species on the soil. Brief descriptions and

a key to the species of lichens found on the reserve are appended.

LICHENS FROM THE T. G. B, OSBORN VEGETATION RESERVE

AT KOONAMORE IN ARID SOUTH AUSTRALIA

by R. W. Roceks*

Summary

Roeers, R. W_ (1974).—Lichens from the T. G, B. Osborn Vegetation Reserve at Koonamore

in arid South Australia, Trans. Ro Sec. S. Aust. 98 (3), 113-123, 31 August, 1974.

The Koonamore Vegetation Reserve has a hchen flora of at least 38 Species. The level

of endemism (19% confined to Australian arid regions) is lower than that in other nrid lands,

bul the total number of species is similar to that found in the arid lands of Asia and North

Africa, and the percentage of foliase species is higher. It is possible that either the environ-

men{ al Koonamore is less harsh than other areas with similar rainfall, or that Australian

foliose species are more drought resistant than those from olher areas. However. the braad

species concept followed here, and the topography of the reserve also, tend to limit the number

of erustose: species, All soil-surface species accue more frequently om loamy soils than on

sundy soils. It is suggested that Collema coccophoras, Dermatocarpan lachneum, Endocarpan

pesillanm and Heppia latosa, the species most common on sand and most commonly occurring

alone, are the pioneer species on the soil. Brief descriptions and a key to the species of lichens

found on the reserve are appended.

Introduction

There have been a number of recent studies

concerning lichens in arid southern Australia

{Rogers 1971, 1972a, 19726; Rogers & Lange

1971, 1972); however. these have dealt only

with species growing on the soil.

The T. G, B, Osborn Vegetation Reserve at

Koonumore (139°27’'R, 32°15/S) was, estab-

lished in 1925 to study the regeneration of

over-grazed arid shrubland, this work being

summarised by Hall, Specht & Eardley (1964).

Although it is only small (390 hectares), it has

4 vegetation representative of much of arid

South Australia, The Reserve ts loca(ed in an

area where vegetation formations of the more

arid, Jow, open shrublands to the north occur

wdmixed with fornialions from the low wood-

lands to the south, The Reserve has. a rainfall

of only 182 mm per »onum, and, using the eri-

terig of Meigs (1953) is Arid.

The only report concerning lichens from the

Reserve is: in Osborn, Wood & Paltridge (1935).

The collections were made by C. Barnard, and

Specimens sent to Kew for determination.

Examination of the material retained as. dupli-

cates in the berbarium of the University of

Adelaide (ADU) shows that some ef the con-

fusion in the discussion of lichens by Osborn,

Wood & Paltridge was due to limited knowledge

of lichens and their structure,

The “undetermined species of Acarosporu”

referred tu as forming patches up to § cm in

diameter is, in the specimens retained, mostly

lurge colonies of Diploschistes scruposus. How-

eyer, in a few cases, small, fertile thalli of .4.

smaragdula (rarely 2 em in diameter) are pre-

sent in the crust of 2. serupasus. It is probable

That similar material was sent to Kew, and the

obviously fertile Acarespera, but not the often

sterile Diploschistes, determined. Two of the

three other soil-surface species discussed as

being conspicuous. because of their apothecia,

are not so, Lecidea decipiens has small pink

stqjuamules with a white edge, and rarely, black

marginal apothecia. Osborn, Wood & Paltridge

upparently mistook the small thallus Tor an

apothecium. Similarly, they confused the thal-

jus of Dermatocarpon hepaticum with \apo-

thecia: D. hepaticum has immersed perithecia,

not apothecta,

During 1965-1971 the Reserve was visited

frequently by the author who collected speci-

mens for lichen studies.

*Kolarny Department, University of Queensland, St. lucia, Old. 4067,

114

The Lichen Flora

‘the soil lichens at Koonamore are a siriking

feature of the Reserve. Over much of the area

the lichens form a continuous carpet, which is

rich in species, Many of the small calearcous

pebbles on the soil surface are completely en-

crusted with lichens, often with a variety of

species on a pebble no more than 1 cm in dia-

meter, Bark and wood of live or dead trees and

shrubs supports a usually sparse growth ol

lichens.

From the collections made in 1965-1971,

and from collections housed in the Botany

Department, University of Adelaide, 38 species

in 25 yenera were determined by reference io

the literature and herbarium material, These

ate listed in the Appendix. The flora is eam-

parable in number of species to that found in

south-western Africa (41 species, MDoidge

19501, in Arizona (33 species; Fink 1909) and

in the Negev (37 species; Galun & Reichert

1960).

Brief descriptions and a key to the species

from the Reserve appear in the Appendix.

Biogeographic Considerations

Weber (1962) commented on the similarity

of sri vone lichen floras from various contin-

ents. Rogers & Lange (1972) illustrated this

by reference to the soil-surface lichets fram all

continents except South America.

in desert areas, the genera Acaraspura, Aspi-

cilia, Ruellia, Cajoplaca, Collema, Dermato-

carpon. Endocarpon, Heppia, Lecgnore, Rino-

dina and Verrucaria daminate the lichen flaras.

All these genera are crustose. "The most coim-

mon foliose genus is apparently Physeia, bub

Parmelia, Teloschistey and Xanthoria are also

R, W, ROGERS

widespread. All of these genera are recorded

in the Reserve although it is likely that the

records fot Ritedina und Buellia ave based on

identical material (see corament in species des-

criptions).

Literature was searched to see whether the

species occurring at Koonamore grow in other

deserts, Reports were placed into four regional

groupings: North America (Fink 1909, Herre

1911, Rudolph 1953, Weber 1963), North

Africa (Faurel, Ovenda & Schotter 1953),

western Asia (Steiner 1921, Lamb 1936,

Svatala 1957, Galun & Reichert 1960, Poelt &

Wirth 1968), and southern Africn (Doidge

1950),

Of the 38 species found in the Reserve, tour

occur in each of the other four desert regions

considered, These are Avarospara suhleichert,

Caloplaca murorum, Dermatoearpor lachrenn

and Lecidea decipieny. A further four species,

Endocarpon pusillum, Parmelia pulle, Physcia

stellavis.- and Toninia cvoeruleontgricans occur 10

three of the four regions,

The seven taxa (19% ) asterisked in Appen-

dix II are endemic to Australia, wiih the excep-

tion of Chondropsis semiviridis. and Parmelia

reprans, which alsa occur in New Zealand, This

is lower than the 30% endemism recorded by

Faurel, Ovenda & Schotter (1953) fog the Sa-

hara, and similar to the endemism reported by

Galun & Reichert (1960) for lichens [rom the

Negev, Israel. Of the other species, 18 (43% )

are also found in North American deserts, 1-1

(37%) in southern Africa, 11 (28% ) in west-

em Asian deserts, and & (21%) in the Sahura-

Comparison with floras from other atid lands

(Table 1) indicates that the flora ut Koonamore

is unusually mich in foliose species. The most

TABLF, 1

Life-forns spectra for the lichen population in desert regions, with ather South Australian

specina far coaMmiparixven.

Ee EEEt ttt

Location

% cruslose

and squamulese % foliase = % Fruticase

Koonamare

Reno (Herre 1911)

Tucson (Fink 1909)

Negev (Galun and Reichert 1960)

Sahara (Kaurel, Ovenda and Schotter 1953)

Acid South Australia*®

Semi-Arid South Australia*

‘Temperate South Australia"

AIL of South Austtalia®

species species Species

58 42

75 25 0

9) 9 0

9) 6 2

97 2 a

7S 23 2

57 55 8

37 4] 22

45 36 19

Nisin mcs apc bali sk as

"Rogers. R, W, (1971) Unpublished Ph.D, thesis (University of Adelaide} Apperstix J,

pp, 183-186.

LICHENS FROM KOONAMORE lis

directly Comparable area is that studied by Fink

(7909) at Tucson. That arca was somewhat

larger with more diverse substrates and a

slwhtly higher rainfall. The area studied hy

Herre (1911) ut Reno included aw altitudinal

range of several thousand feet, alsa with a

higher rainfall than Koonamore. Both of these

areas were, however, poorer in foliose species,

From Table J it is alse evident that the Koona-

more Reserve is relatively richer in foliose spe-

cies than and South Australia taken as a whole.

Kenaut, Marrache & Troter (1968) cxa-

mined the use of lichen life-form spectra as

liidicators of avidity, With 42% foliose species,

Kooninrore would rate as suh-humid or per-

haps semi-arid on their scale whereas it is

vhissed as aril by use of climatic indices

(Meizs 1953), AL first his suggests that either

the climate at Koonamore ts Tess harsh m reta-

Hon to its eainfall and teoyperature regime than

other desert regions. or that southern Austra-

lian foliuse lighens ure more dronglit resistant

than their counterparts elsewhere. However, the

relatively high percentaye of folioxe lichens on

the Koonamore Reserve may be duc in part to

the ahsence of cautcroppine rocks m the area,

Two species absent from che Reserve, but

which occur on rocky outerops in the mearhy

Yunta and Waukarings hills, are Dfplaschisres

avpsaceans (erustose) and Heppia euploca

(squamulose!. Another factor may he the

broad species <oncept followed in naming the

Kuonamore Jichens, While many taxonomists

will not aceept the revision ot Acawraspera sub-

rgenus Xanthothallia by Weber (L964), in which

about 80 accepted species were reduced tn two,

his conclusion that the nunvher of ¢rustose

lichens from arid areas is greatly inflated by

description of envitaninental modifications as

distinct taxa (Weber 1962) is sound. Apart

from the genus Acurospora, the genera Leca-

nwraand Leeldea have also been split to accom-

modale Wumerous environmenial nindifications.

It is likely that other authors have followed

ralher narrow species concepts, increasing the

total nomber and hence proportion. of crustose

species gecorded fromy arid fands. This may

also explain the similarity with the Narth Ame-

tical) desert lichen flora, siace both the present

author and North American authors have fol-

lowed a siinilar hroad species concept.

Ecolory of Soil Surface Species

To study the soil-surface lichens, 26 transects

were randomly tocated in the physiographically

diverse south-eastern half of the reserve, Along

each transect, ten 15 cm by 20 cm quadrats

were laid at random intervals belween vero and

ten melves apart, atid the soil surface lichens

within the qnadrats listed, The soi type was

classified fnto one of two categories, calcareous

loam or sand.

Thirteen taxa occurred in more than ten of

these quadrats; these are listed in Table 2, aleng

with their frequency in loamy and sandy

quadrats. OF {he 260 quadrats, 67 were withoul

lichens. Fifty-five of the quadrats without

lichens were on sandy areas, 12 on loamy areas.

Of the loamy quadrai BS% had lUchens.

wherens only 52% of the sandy quadrats dul

The site with the greatest number of specics

{nine} was on loamy soil, whereas the richest

site on sandy soil had seven species. The mean

number of species on sandy sifes beanng

lichens Was 3.5, significantly lower (p<1%)

than the mean of 4.3 on foamy sites with

lichens.

If it ts assumed that there is an incresse m

species diversily 4s a communily develops 11

wards its climax composition (Whittaker 1953),

then it follows that spectes which tend th occur

#lone are more likely to be pioneer species than

these which tend to occur only with otters

From Table 2, it is apparent that Callema

coccephorus, Fndecarpon puyilluen, Dermate-

carpet lachnewn and Iteppla [tesa are the

species most commenly occurrme, alone, or

with lew others. These species arc therefore

likely to be the pioneer species, ovcrrring early

in successional development on soil surfaces.

A ourmber of sites on the reserve were dis-

covered where lichen Crunts were judged to be

advancing on to previously Uncrusted areas.

This judement. was based on the presence of

scattered squamuiles. at a distance from a deve-

loped crust, the squamules becoming smaller

and apparently younger is distance froin the

crust increased Dermatocarpon lachiteuni,

Endocarpon pusilla and Neppia hilasa were

the species commonly found in such sitnations.

These observations, together with the nbser-

vations of Rogers & Lange (1971) that Collema

coccophorus, Dermatecarpen fachneum, Endo-

carson pusillum and Heppie luiesa are the spe-

cies least affected by trampling of sheep around

walerholes, all point to the same group of spe-

cies as che pionecrs in lichen succession on and

sotls in South Australia.

The distribution of lichen crusts in relation

to shrub coverage was studied on Quadrat 100,

an arca of 100 m* of fine, calcareous soil on

which regeneration of Atriplex spp. has been

lh RK. W.

ROGERS

TABLE 2

Frequency of sdil-surface species on loamy sotls and sandy soils. fram the Koonamore

Vegetation Reserve, and the frequency with which these were either the ouly species in

a quadrat, or were with only one other species,

Frequency on

Species losm

Acarosporq smaragdula 4

Aspicilia calvarea (¢rustose) 34

a. calcarea (frnticosc ) 18

Chondropsis semiviridts 1

Catlema cocvepharis 35

Dermatocarpen lachneum 63

Endocarpon prsillrore 43

Fuleensia subbracteata 24

Heppla polysporc 35

Mf. liteva uM

Yecidea crystallifera 20

L. decipiens 64

Toninia coerileonigricans 13

Frequency on Number of occurrences

sand. alone with one other

0 a

72 | 2

| 0 1

U U a

44 14 Is

1 z 4

35 3 IS

12 a 1

3 {} |

18 | 6

a u 2

19 tl z

12 i] i

studied since 1925, On this quadrut it was pos-

sible in 1969 to find areas on which no peren-

nial plant growth had been recorded in the past

44 years. These areas were without lichen

growth, On areas with mature perennial shrub

growth,.a lichen crust had developed; the older

the shrub stand, the more developed the lichen

crust. A few areas were found in which the

shrubs had virtually all died: in these the lichea

erust remained intact. [n yet other areas, young

shrubs were starting to Brow on areas quite

devoid of lichen growth.

It is apparent from these observations. that

the lichen crust develops on fine calcareous

soils only after a shruh cover has been estab-

lished, thus stabilising the soil, However, it is

also apparenr that the lichens ate able to pre-

vent erosion of the soil onze the shrub cover

has disappeared. Lichen crusts thus increase the

stability of desert soils: they cannot themselves

stabilise an actively eroding surface.

Acknowledgements

Mr. R. Filson of the National Herbarium,

Melbourne, assisted with many determinations

and commented on the munuscript, He parti-

cularly drew attention to the consistent mis-

determination of Bambylivspora dominyensis

var. durantiuca as Caloplica aurantiaca by

eatlier Workers.. Access to the lichen collection

and library of the National Herbarium, Mel-

bourne, greatly assisted in checking determina-

tions. Responsibility for the names used, must,

however, remain with the author. This study

was. commenced in the Botany Department,

University of Adelaide.

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Appendix

Il, KEY TO SPECIES

1), Thallus fruticose--i-c. without dorsiventeal

differentiation ., ,

1, Thallus foliose, squamulose or crustese—ie

with dorsiventral differentiation . 2

2. Thallus foliose or squantulose either free

from the substrate, or atkiched to it by

thizoids, but with 1 distirict lawer surface 3

2 Thallus. crustose, attached ta the substrate

and inseparable frum it, no lower ‘surface

discernibic, or thallus absent 29

Thallus foliose, i.e. of clongate, often branched

lobes .., 7

Thallus squamulose, je. of round to ovoid

sciles which nay be crowded together ra)

Fruticost Sricres

4, Thallus gold io grey, on wood or bark ..,

Teloschistes chysophthateiuus

4, Thalliis grey, black or dark olive green, on

rock Or soi Po 2 5

S, Thollus grey, of anustomosiog eylindrical

lobes... Aspietlia calcurea

§ Thullus black or dark olive preen, the lohes

hot anislomosing 6

6. Thallus of cylindrical lobules or fattened

lobes up to 5 mm high, forming a rosette

Callenta caccapharus

6, Thallus of cylindrica) lobes op te 2 mm

high, the individuals densely packed to

form an apparent crust

Syralissa symnphorea

FOLIOSE SPECIES

4% Thallus black or dark olive green, eclalinoue

when wet , .. Collema caccapharer

J. Thallus not black nor gelatinous When wet ., 8

8. Thallus bright yellow, gold orarange 9

&. Thallus olive, grey, blue ar

yellow-green 2... .. re-, stl

9. Thallus of minute, flattened, ecillate Imbes

(less than 1 mm broad), upper cortex K—

Candelaria concolor

S, Thallus of broader tobes, sumetimes ciliate,

Upper coriexn K+ burgundy 10

10. Lobes. eciliate, appressed to the subrdtrite

Nanthorie ev ined

10. Lobes cihate, ascending from the substtate

Teloschistes chrysophthatmas

Vl. Upper surface yellow green. 4 4, . 12

1]. Upper surface grey, blue or olive If

12. Thalluy rotting into a ball when dey, on-

rolling: When wet .

Chondrapsix semiviridis

12. Thellus not colling andl unvolling . .. 13

13, On soil surfaces 14

13. On rocks, wood or bark 4. 0. wy TS

14, Thallus freé on the surface, much distorted

and convoluted Parmeélia convoluta

14. ‘Challus attached to the surface by rhi-

zoids, Inhes slightly convex, appressed -

Parmelia repians

15, hn woot or bark .., Parmelia ferax

15, On rocks Parmelia cf. lineola

16. Thallus olive oo... ., eee: 17

16. Thallis blue or grey 18

17, Lobes I mm broad or fess... . tine oh

Physciopsiy syncella

17. Lobes more than 1 mm broad -.-

Parmelia pulla

18, Lobes more than 3 mm broad

t Parmelia subathicuns

18, lobes less than 2 mm bread 19

19, Lobes with murginal'soralia - a ia albicans

19. Tobes esorediate - , 20

20. Medulla K+ yellow - ey

20, Medulla K—_.

Physcia alba

. Physeia stelluris

SQUAMULOSE SPECIES

21, Phycohiont blue-green . 22

2). Phycobiont ercen =. 3

22, Squantules elonpate: margins granutgr but

not thickened, forming 4 rosette

Heppia lutase

crenate, margins

thickened, not forming a rosetie

Neppia palysgoru

22. Squamules ovold oy

smooth,

LICHENS FROM KOONAMGRE

23. Squamules orange (@ red, offen with a white

Margin ,, : oldest decipiens

23. Squumules brown, black, erey-green «'

prey, . sie tm «oe 24

14. Squamules thin. pale grey-green, che mur-

Lins Celine up when dry pee

Cladania sqguamiules

24, Squamules thicker. brown, black or prev,

the margins not curling bp when dry = 25

25. Asei in perhecia immersed in the thallus 26

25. Asc) if spottecia sessile on the thallus 28

26 Spores muriform, algae in the hymenium

Fiidnearpon pusillim

ih. Spores not septate, algae absent from the

hymeniua : ry oss 27

27. On soil. sqnamules brown 2-3 mm across

Dermiatocarpan tachneum

27, On tack, squamules black less than 1 nm

Aeros DBermuoeparpan COM paclient

TX Squamules pale grey or brown, epruinase,

the upper surface deeply cracked, giving

x crystalline appearance, apothecia small

in relation toa the squamules ., .

Lecidea erystallifera

24. Squamuics dark grey or black, often

truinose, the upper surface shallowly

cracked, apathecia large in relation to the

sauamules _-._ Tontnia coeruleonigricans

CRusTasSE Srecits

29. Thallus or apothecia yellow or orange 3d

29. Thallus and apothecia devoid of orange or

yellow coloration 2 _ 34

30. Thallus with small but distinct marginal

lobes + ove Ol

30. Thallus withoat disting? marginal lobes or

thallus absent. , 32

41, Thallus smooth, orange to orange brown

Calaplaca myrofion

31, Thallt's mealy, very pale yellow when dry

becoming bright yellow when wet ,, rs

Fulzeasa sullbracteata

32. On rocks or soil, spores. more thin 64 per

ascus P .. Avarvaspora schleighers

32. On wood, spores § per usetis . 33

33, Apothecia bright yellow, (halls absent or

only u prothallus present

Condelariclla antennarin

33, Apothecia dull orange, thallus of greyish

areoles Bombyhospora domingense

' var, aunxantlaca

34. Crust black, OF minute squamules or

minute fruticose Tnuividuals closely

packed Se Ene Sou 35

34, Crost white to brown, sometimes preolate

or granular, bt not squamulase on feutt-

cose Individuals $e. 46

35. Thallus eclatinows when wet, individuals

minutely frutieose about 0,1 mm diameter;

usci in apothecia . , Synalisva sympharea

Thallus not gelatinous when wet, individuals

squainulose, usci in perithecia .

Dermatocarpan compdcinm

30 Spores 64 or more per ascus ., 37

36. Spores less than 16 per ascus vo 3B

37. Thallus brown, without marginal lobes,

Ustially one spothecium per ureole, on rock

Acarospara cervina

37, Thuallus grey, with distinct marginal lobes,

apathecia usually several per areole, on soil

and rock ow Acaraspori sriaragdita

38, Asci in perithecia, thallns virtually indis-

tinguishable fron: the substrate Pe...

Verrucaria cf, caleiseda

38, Asci in apothecia, thallus quite distinct

39. Apothecis immersed or adnate on the

thallus. _ - piste es 40

39. Apothecia seysile on the thallus gz

40, Apolhecia 3 mm or more in diameter _.

Diploschistes agetlatues

AQ. Apothecia Jess than 2 mm diameler 41

41. Spares black or brown nee age = .

Diploschistes seruposus

41, Spores hyaline... ... 2... Aspleilta eqtcaren

42. Spores black or brown .. Brellia subalbula

42. Spores hyaline .., Lecunora sphaerospora

1. DESCRIPTIONS OF THE SPECIES

dcaratpora cervinw (Ach) Mass. 1652228,

Lecnnora cervina Ach. [RI4: E88,

Thallus of small (1-2 mm broad) brown. squa-

mules with white margins, usually scattered but

eceasionally compacted. Apothecta immersed,

ptuinose, usually one per squamule. Spores many

(100) per ascus, non-seplate. }

Occasional on small calcareous pebbles, Speci-

men examined*: Rogers, 24.01.1969.

Acarosporu schleicher (Ach.) Mass. 1852:27-

Urceolaria schleicheri Ach. 18107342,

Thallus of minute (<1 mm diam.) sulphur

yellow squamules, usually scattered, but sometimes

hecoming areolale, Apothecla immersed, one per

squamule, Spores many (100) per aseus, non-

septate.

Rare, found only on silicious pebbtes at Koona-

more, bul may: also occur on compacied soil, Speci-

men cxamined: Womersley, 6,vi.1946,

Anerson smaravdaule (Wablenb.) Mass, 1852:

Ebdocarpon smarasdulien Wahlenb. apod Ach

1803:29,

Thatlus of small (7-2 mm Jn diam), chalky

white to brown squamurles, forming plaques up to

2 cm in diam, Apothecia immersed, sometimes

Proinose, one to five per squamule, a well deve-

loped exciple concolourous with the thallus, Spares

many (>100) per ascus, non-septate.

Common on calcareous soil surfaces, often with

Diptoschistes scrrposas. Specimens examined:

Barnard, 12.xii.1927; Anon... May 1943; Eurdley,

June 1946) Rogers, 20.xi.1967,

“ Specimens cited as Regers ure in the author's private herbarium, wl alhers in the berburium of the

University of Adelaide (400).

120

Aypicitia calcarea (L.) Mudd 1361; 161.

Ciehen calearens L.1753)1140,

Thalius white to greyish, either urustase ar more

or Jess fruticose; if crustose then arcolute, it fiuti-

cose the lobes cylindrical, psendocyphellule, ana-

stomosing, 0.5-1.0 mm thick. Apothecita known

only on crustose forms, Jmmersedl with a crenate

margin, the dise densely pyruinese. Spores 2-8 per

AscUS, Mon-septale.

Virtually any calcareous pebbig of the reserve

jas the crustose Torin om it samewhiere. “Lhe fruti-

cuse form is less common but occurs mest often

al the junction of pebbles and soil. Both forms

also accur on calcareous soil alone, Nunterovs

intergrades. have becn observed on the reserve.

Specimens eaumined: Anon. May 1948; Rogers,

Fx. 1967,

Bombylieryora tlontingersts (Pers.) Zahlbr, var-

avcontiaeca Zahlhr.. in Magnussan & Zahlbruckner

1945:32.

Thallus an obscure yellow-prey: crust covering

extensive urcas on old wood. Apeihecia orange,

<1 mm in diam, very fumnerous, sessile, convex.

Spores 8 per aseus, usually 5 septute,

Very common on-desd, decorlicale Iwigs. espe-

cially wf Cusste spp. and Ererntophila spp, where

entire branches may be covered. Spocimens eaxa-

tolucd: Barnard, 12-XxiU.1927, Rogers, 5.231967.

Buellia subalbila (Ny) Muell, 1880:79,

Lecilea subalhula Nyl, 1868516,

Thallus » white, areolate crast forming patches

up io Scm indiam. Apothecia black, up to 1 mm

in diam., numerous, sessile, convex, with a false

white exciple disappearing carly in development,

Spores 8 per ascus, black, seplute-

Wery common on calcareous pebbles. Specimens

examined; Anon,, Sune 1946; Anon., Muy 1948;

Rogers, 24.11. 1969,

Although the material has nat been examined |

is likely that specimens determined at Kew as

Rinedina diffractella Muell, for Osborn, Wook &

Paltridge (L995), was identizal with the napterial

here called #. subulhila. The bvo species are very

similar wecording to their descriptions, cach having

a thalloid exciple when young, which disappears

with) acc, hence confusion about the appropriate

genus for the material. The species differ, however.

in that there are slightly Jarger spores (!2-12.6 x

5.7--4 wn) in Bo subalheta than in R, diffractelta

(7-10 x 4-4.5 pn),

Caloplawe murorin (Holtm) Th Pr

Lichen murvrvit Hoffer, |784203-

“Lhallus crustose, arevlale at the centra, some-

times with distinc, marginal Inbes |—t nm long,

or the thallus o£ verrucose Squarciiles, light arange-

hrown. Apothecia sessile, the cise olanee to rusty

brown, the exciple concetonraus wilt tre thallus.

Spores % per aseus, polari-hilocular:

On siliceous rocks, not common. Specimens exa-

mined: Womersiey, 6.411946; Anon, May 1948-

Candelaria conculur (Dicks,) Stein jn COL 187)!

18712170,

Lichen conceloe Dicks. 1793: 1R-

‘Lhallns yellow, minutely foliose, lobes 0.1-0.5

maint tread, « I mm. long, forming rosettes of

R. W, ROGERS

spreading irregularly. the margins irregularly gra-

nulur, Fertile specimens have not been found in

South Australia, According ta Osburn, Weod &

Paltridge (1935) this specics iy uncommon, but

forms extensive patches an twigs. This specics bas

hot been relocated by recent collectors despite

cateful examination of the area.

Record: Barnard. 12.11.1927 (not seen)

Candelariella antennaria Ras. 19392137

Thallus missing. Apothecia sessile on the sun-

strate, the disc and exciple greeaist yellow. Spores

§ per ascus, gun-seplote. Paraphyses xeplate, sonie-

times branched.

A cominon but obscure species occurring ad-

mixed with Bumbylivspara domingense var. cdurat-

face on wood. Specimens examined) Rogers.

2211x1969, Ragers, 141,971.

§Chundrepsis semiviridis (T Muell. ex Nyl,) Nyl-

ex Cromb. 1880:397.

Parmnelionsis semiviridiy F. Muell ex Nyl 1885:

57.

Thallus foliose, creen above, pule yellow-brown

helow, lobes 3-5 mm broad, strictly dichnlameously

branched, rolling into a ball when dry, lying flat

when wel Apothecia extremely rare, sessile, dise

brown, exeiple cencoluurous with the thallus.

Spores &, woo-scptate,

At Koonamore ihis species tas lobes approach

ing 5 mm wkle, passibly the broadest form found

in Australia, Common on soil surfaces in scattered,

patehes. Barnard apparently did not find this dis

finctive species on the reserve in 1927, Specimens

examined’ Anon, May 1942; Barren, 71944;

Ragers, UNL 9I6B.

Cladenia Sp.

Schilered squamules grey green above, whine

below, without padetial development,

Very raro on shaved sail under Meteradendruny,

Specimen exnmined: Rogers, 8.x. 1967,

Ceallema coccepharura Tuck. TR62~385,

Thallus a rosette of deep olive lo black crenare

fobes 2-3 mm Jong. much convoluted, sometimes

wilh cyliedrical lobules, gelatinous when wo, Aji.

thecia Tot comtmon, about L mm broad, the disc

and exciple concoloraus with Li thallus. Spares €

pet Ascus, ONCE sepPlate

Jofreqnent, om culeareatis oe sandy soil. Sprei-

men examined: Mapers, S.xi7,1967,

Denmatecarnan curpacen (Mass) Teltan, 1912:

52.

Placidinat cempuviin Mass, 1836:32,

‘Vhallus of minute (0.2-0.3 unm) squamules

fucked together forming a dark brown playtic

Petithecis. opening by pores, sporés & per asscris

non-septate-

Common, hut itcunspicuows on calcarsous

pebbles, Specline examined: Ragers, 9.1x.1969,

Derniarocarpan tached CAch) Smith 191) :270.

Lichen lochnens Ach, 1798:140.

Vhallus of lan to dark brown squamules I-27

mm accass, initisly ovate, entire, plane to slightly

convex bul becomine crénate and distorted with

uve The rhizoids of this species remain fine, per-

mifting IL ws be distinguished From the coarse

LICHENS FROM KOONAMORE IZI

rhizined Endecarpen pusilion, Perithecia opening

hy pores, Spores & per ascus, non-seprate-

Common and consprcmous on calesreous soil,

superficially like Endocarpon prsiliim. Specimens

examiiied) Barnard, V2.50,1927: — Regers,

20, xi, 1967,

Diploschistes avefarus (Vil) Norm. 1853:232-

Lichen wwellatus Vill 1789-988.

Thallus an extensive while crist of smoath,

chalky arcoles up ta 1 mm broad. Apothecia

poorly developed or absent on the seserve, but

sesallé with a dick thalloftd exciple and 2 blick,

fist disc. Spores 8 per sscus, black, oniriform,

A tare, but quite striking lichen on calcareous

soil in deeply shasled sites. Specimens cxamined:

Actin, | Stay 1942; Hurdley, June 1946: Revers,

Mi .

Diplaschistes serupasvs (Schreb.) Norm. 1853:232.-

Licher scrapesws Schreb. 17717133,

Thallus aa extensive Moury ercy or white crust

With aregies << mm across. Apothecia very com-

mon, immersed, ¢, 0.5 Jum ja diam, the dise black.

Spores 8 pér ascus, black, murifarm.

Comman on calcoreous soils. Specimens caxa-

Muned: Barvard, V2xi.1927: Berdley, Iune }946:

Rogers. 20.x1. 1967.

Endavirpan jpesitlaen Hedw. 1789:56,

Thallus of brown, usually crenate, squamules

with extensive rhigoidal and stolon development

helow. Perithecia immersed, opening by a black

pore on the upper surface. Spores usually 2 per

ascus, black, muriform,

Common on caleaicous soils and firm sanis,

easily confused With Derménivarpan lachnetm,

Specimen examine: Kogevs, 20.Xi,1967,

Fulgeasia. subbracieata (Nyl.) Poel 1941, na 137

Tecanore swbbracteata Ny 1885:534_

‘Thallus crustose. somewhat grinulur, very pale

yellow when dry, bright yellow when wel, the

Mains showing minule lobes Apolhecia adnate,

rare, the exciple colored like the dise, deep rusty

brown. Spores 8 per ascus, Nun-septaue.

Rare, on sandy and calcareous soils, Specinica

examined: Rogers, 2.41969,

Heppia lutesa (Ach) Nyt, 1K#S;45.

Collerta titesum Ach. 1814:309.

Thallus squumulose grey-green to olive, squa-

mules forming snail rosettes (5 gim in diam.) the

Mmuareins ganular, Apotheciu immerses, sually one

per squamule, disc ved. Spurcs 8 per seus, mion-

septate.

Common on calcareotts salle Specitron cava

mined; Kogers, 4.¥ii.1969,

Heppia padyspera Tuck, 18822115,

Thaltus squamulose, fan tn alive, squamules 1-4

Mm it diane, round oF crenate with & thickened

margin. Apothecla usnally one per squamnle,

immersed, the disc red. Spores many (>32) per

ASCUS, NON-septate,

Common, bul very obscure on sandy and cal-

carebus soils. Specimen examined: Rogers,

4vii 1969,

*Lecanora spheeraspore Muell, 1892:L96.

Thallus crisiose, white to grey, areotate, areoles

up to | mm la diam, Apothecia sessile with a white

margin, Usually cronale, the dise grey, al first flat

then becoming trarkedly convex, Spores § per

ASCHS, NoN-seprate,

Very common on calcureous pebbles, Specimens

examined: Reapers, §.xiL,1967) Rocers, IU,ViL96S,

*ecidea crystalfifera Tayl, 18471148.

Phallus of grey-brown squamoles |-3 mm

broad, enlire to crenate ar sarmewhat lacerate, the

upper surface sculptured inta 4 ahasy of pyramid

like solid angles, giving if a crystalJine appearance,

Apothecia not found at Koonamore, bul sessile,

flat to convex, the disc dark grey lo black. Spores

§ per ascus, non-septate,

Very common att valcareous soils. Specinicn

examined: Rugersx, 20.41.1967,

Leelded decipiens (Hoffm.) Ach. 1803:80

Psora decipiens Haoffm. 179468,

Thallis of pink squamulcs 1-7 mm broad, the

Inargins or the whole thallus white pryinase, the

squamules entire to crenate of lacerate, often

maskedly concave at the contre with deflexed

margins. Apothecia rare, marginal, sessile, the disc

Mack. markedly convex, Spores 8 per Asctis, non-

scplale,

Qne of the most common and obvious lichens

on soil in the reserve. Specimens examined: Har-

add, 12.4%01.1927, Anon, 1-i¥,19392; Fandlev, June

1946; Rogers, 20.xL,1947.

*Parmeli cenvaluta Kremph, 88i;347,

Thallus yellow-green ubove, fohiesc; the lower

surface light brown, sparsely rhizinate, usually con-

cealed within the rolled and convoluted Jobes, the

older fobes offen rugose above, up la 5 mm broad,

Aputhecia very tare, sessile, the disc hrawn, the

iargin yellow green.

This species is separated from the very similar

P. -australivnse by the prescnee of Salicinic acid

(medulla K— yellow becoming red) whereas J”,

wusrraliense Jacks salicinic acid and 1 Therefore

K— {Kurokawa 1969). Mixed populatinnys have

heen fonnd in some places, tut all Koonamore

Material exumined 8 FP. convalned.

Common, lying free on the soil sarfice Speci-

mens exainined: Bartard, 12.xi1.19272 Anot., Muy

1942; Rogers 20.x1.1967, Rogers, 17.4969.

*Parmelia ferax Mucll, 18861257.

Thallus yellow-green above. foliose. the lower

surface black, sparsely rhiainate, lobes 0.5-1.5 min

broad, margins crenaie, branching irregular, Apo-

thecian common, margin oolared like the thallas,

the disc brown. Spores 8 per ascus,, non-septate.

Parmilia ferax may he confused with P. rretideta,

hut it has «4 more rugose thailus, has no K-| acids,

and produces physodalic not protocetratic acid

(Kurokawa 1967),

Common on dead twigs and bark of trees. Speci-

mens examined; Barnard, 12.xii1,.1927; Anon., May

1942. Womersley, 6.¥i.1946; Rogers, 20.xi.1967.

Parmiclia ¢f, lineata Berry 1941:77.

Thallus yellow-green above, foliose, the lower

surface pale to dark brawn, closely adnate to the

subsitale. lobes 2-5 mm broad, sub-iichntormous,

422 R. W. ROGERS

the upper surface becoming rugese and cracking.

Apothecis nat xecn.

The subgenus Nenrhaparmelia ta which ibis

material belongs is complex and poorly undet-

stood. Absence of isidia and Soredla, and presence

of salicinic acid, place this species clase to P

finedla, a western North American spzeics,

Rare on quartzitic pebbles. Specimens examined:

Womerstey, 6.vi.1946; Anon, May 248, Rogers,

Zhe 47,

Parrteliy pulla (Schreb y Ach, ISl4)206

Lichen pullus Sehreb. 17715131.

Thallus dark olive or brown above, foliose, the

jower surface dark, lobes 1.5-3.0 mm broad.

sparsely rhizinale. the Margins crenale, branching

irregular, Apathecis rare, the margin curicvolorans

with the thallus. dise dark brown, Spores & per

HSCs. NON-seplate.

Rare, of deeply shaded culeareouy soils and

rocks, Specimens examined! Wantersley, 6.vi. 1946:

Anon. May 1948,

“Povmelin reptans Kuok: in Baker et al. 19732137-

Thallus yellow-preen above, foliose, forming

rusettes [-3 em in divm. mere or Jexs dicholu-

mausly branched, lobes Nnear, 0.7—2.0 unm broad,

lower surface pale brown with lang blick rhizoids.

Apothecia unknown.

Very similar to #, auiphixautha Muacll, bow-

ever Po reptans tends to jrnve wider lobes (P,

amphixactha up ta Emm) and has fumaprote-

cetruric. succinprotocetraric and usnic acids (Pa

yellow turning crimson) whereas 2, aipltsentha

has furslictic, stietic and usnic acids (Pd yellow)

(Hauker et al, 1973).

On soil, weuslly in deep shade. Specimens ¢xa-

mined: Farnard, 12-x11.1927; Earilley, Tune, 1946.

*"Parmiclia subaltiedis Stitt, 1877-7$:254.

Thallus grey-blie, foliose. light brawn below,

lobes 1.5-4.0 mm broad, sparsely rhizginale, the

margins irregular, branching sub-dichotomaus.

Aputhecia common, the margin concolorous with

the thallus, dise brown. Spores & per ascus, non-

septate.

Very common on bark and dead twigs, tsuully

with Ff. ferqy. Specimens examined: Anon. May

1942: Heorwestey, 6.411946, Ragers. Wax 1967.

Physcia atba (Pee) Much. 1887;12.

Parmellg alha Fee (824: 115.

Thallus erey-blue, foliose, forming distinct

rosettes. closcly. adnale, lobes up to 3 mm broad,

without soredia of isidia, pole below. Apothecia

common, the margift concoloreus with, the thallus,

dise brown, asually pruinose. Spares & pee ascus,

once septule, brown. Cortex K+ yellaw, Pd-+

yellow. Medulla K+ vellaw, Pd+ yellow.

Rare on the bark of trees, Easily confused with

PR, vtefldtels in the field. Specimens examined;

Anon, May 1948.

Phyycia albicans (Pers) Thoms. 196388,

Parmelia albiewns Pers, 1211517.

Thatlus blue fo samewhat olive, foliose, form-

ing distinct rosettes, closcly adnate, lobes 1-4 mm

broad. enntiguouy to the margin with ascendent

lubtifunnt soralia; pale below, becoming dark,

Apothecia rare. Ypores B per asums, once seplile.

brown, Cortex K+ yellow become red, Pul—

medulla K-- yellow hecoming red, Pi—,

Rure, found on the bark of Cuswuriia cristata.

Specimens examined: Anon. May 1948; Royers.

20,X1.1967,

Pheseta siellaris (Ach. Nyl. 18562307.

Parmelia sietlarixy Ach, V8103:209,

Thallus blue-grey, foliose. forming rosetces. or

extended pitches, not closely appressed, lobes (.5—

1.5 mm broad, without isidia or soredia, pale

below, Apothecia common, the margin coloured

like the thallus, the dise brown, often bluish

pritinose. Spores & per useus, pice septate, brown,

Cartex K--vellow, Pd—: medulla K— Pd,

yellow brown.

Ou the bark of trees, not cammon. Specimen

exumined: Rogers, 20.01.1967.

Phosciopsis syncolla (Tuck.) Poelt 1965230.

Pheyscia syncotla Tuck im Nyl, 1838428

Thallus brown, foliose, Forming extensive

putehws. closely udmaic. lahes about 1 min braad,

dark below. Apothecia up to 1S mim broad. the

marsin concolorous with the thallis the dise

brown, sometimes prujnass. Spores 8 per ascus,

once septate, brown,

Obscure, hur in extensive patches on the barb

of deacio girenes. Specimen examined: Repers,

TK. 1967.

Syneliyvya sympltorta (Ach) Nyl. 18562204.

Fichen ayenphoreus Ach. 17981355,

Thallus dark olive-green to black, minutely

friticose, packed into patches up-to 4.cmin Umm..

individual thalli 1 mm high, less than bE utt in

diam., branehed, the lobes tightly packed, scane-

what nodulate, Apothecia up te 0.2 mai in diam.,

more ar less immersed in the dips of the upright

lobes. Spores usually & per uscus, mon-seplate,

A Very inconspicuous species on calcurouus sil.

Specimen examined; Rovers, 2Ux11967.

Trteschistes chrvsoplihuintins CL.) Th. Fr. 1861-51.

Lichen cherysophthalmus LO 17712311.

Thalluy gold to grey, foliose, forming ia slirubby

clump, the lobes 0.5-2.5 min broad with long mar-

vinul fibrils, with neither isidian nor soredia. Apo-

thecia common. pedicellate, Up to & mm in diant..

with fibrils on the margin, concdlaraus willt the

thallus. Spores & pet ascus, septate.

On twigs of bushes and bark of trees Specimens

examined: Barvurd, 12.xi1.1927; Anon. May 1942,

Toninta coerulronivvicans (Light) Th, Br, 187th:

356.

Lichen coernleonigricons Light! W777; 805

Thallus of dark grey, small (1 min in diatn.)

inflated, reticulutely cracked, usually hlue-priuinose

squumules, Apothecia often larger than (he squa-

mules, the murein ane the disc boil) black, often

prinose, Spores B per ascus, fusifunm. ones sep-

tate.

Common on calcareous and sandy soils, Speci-

mens examined: Barnard, 12.xii.1927, Anon, May

(943: Womersler. 6.41.1%6; Anon. May 1948;

Regers, 30,iv. 1969.

LICHENS FROM KOONAMORE 123

Verrucaria aff. calciveda DC. in M. Lam. & DC,

1805:317.

Thallus a whitish crust, almost indistinguishable

from the substrate, smooth, somewhat powdery.

Perithecia immersed in pits in the thallus, showing

as sunken black spots barely 0.1 mm in diam,

Spores 8 per ascus, 24 wm by 12 »m, non-septate,

hyaline,

An extremely obscure species on calcareous

pebbles, appearing to be a pitted limestone surface

unless carefully examined. Specimen examined:

Anon., June 1946,

Xanthoria ectanea (Ach,) Ris. ex R. Filson 1969:

83.

Parmelia parietina var. ectanea Ach. 1810:464.

Thallus forming a golden rosette, foliose, adnate

to the substrate, the lobes smooth, up to 2.5 mm

broad, the margin raised then deflexed. Apothecia

common, about 2 mm in diam. Spores 8 per ascus,

septate.

Rare on twigs of Lycium australe. Specimens

examined: Anon., May 1942; Rogers, 30-iv.1969,

SALT CRUST DISTRIBUTION AND LAKE BED CONDITIONS IN

SOUTHERN AREAS OF LAKE EYRE NORTH

BY J. A. DULHUNTY*

Summary

DULHUNTY, J. A. (1974).-Salt crust distribution and lake bed conditions in southern areas of

Lake Eyre North. Trans. R. Soc. S. Aust 98(3), 125-133, 31 August, 1974.

Investigations and surveys of salt crusts and the lake bed conditions in southern areas of Lake Eyre

North were carried out during 1972-73, using specially adapted transport and equipment.

The nature and extent of salt crusts in Jackboot and Belt Bays are described. An east-west belt of

watery silt with little or no salt crust, separating the main southern salt crusts from northern red-clay

surfaces, is described and termed the Slush Zone. Progressive changes in crust thickness and

distribution of salt, over a period of 43 years, are described in Madigan Gulf and their significance

is discussed in relation to early unrecorded floodings of Lake Eyre and possible instability of the

lake bed.

SALT CRUST DISTRIBUTION AND LAKE BED CONDITIONS IN

SOUTHERN AREAS OF LAKE EYRE NORTH

by J. A. DULAUNTY*

Summary

Devuunty, J. A. (1974).—Sall crus} distribution and lake bed conditions in southern areas

of Lake Eyre North, Trans. R. Soc. S. Aust. 98 13), 125-133. 31 Auenst, 1974.

Investigations and surveys of salt crusts and the fake bed conditions in southern areas

of Lake Byre North were carried ont during 1972-73, using specially adapted transport and

equipment, The nature and extent of salt crusts in Jackboot and Belt Bays are described.

An cast-west belt of watery silt with littke or no salt crust, separating the main southern sult

crusts from northern red-clay surfaces, is described and termed the Slush Zone. Progressive

changes tm crust thickness und distribution of sali, over a period of 43 years, are described

in Madigan Gulf and their significance is discussed in relaiion to early unrecorded floodings of

Lake Eyre and possible instability of the Iake bed.

Introduction

Lake Eyre North is a large salina approxi-

mately 148 km long, from north to south, and

65 km wide, connected by a narrow channel

at its southern end to a relatively small salina

known as Lake Eyre South. For general geo-

eruphical and geological settings ef the Lake

Evre Basin, reference should be made to Johus

(1963) Wopfner & Twidaie (1967) and

Williams (1973). The investivations described

here ure concerned with Lake Eyre North,

und principally its southern balf including

Madigun Gulf, Jackboot Bay and Belt Bay

(Fig. 11.

The lake bed, which lics between 10 and

15 m below sea level (Bonython 1955, p.

69: 1956; 1960; Wopfoer & Twidale 1967), is

gently tilted from north to south, falling some

4m in 120 km from the northern shoreline to

the lowest areas in Madigan Gulf and Belt

Bay, When flood waters from the Northern

Territory and Western Queensland reach the

lake, they enter wt its northern end and nurth-

eastern side, and flow south across the lake

bed 10 the southern hays where salt is dis-

solved, fine silt deposited, and salt redeposited

on evaporation of the water (Bonython 1956).

This has resulted in the occurrence of crusts

overlying Recent sediments in southerit ateas

of the lake and a red clay surface over its

slightly elevated northern half from which salt

is periodically transferred to the lower southern

half. Small quantitics of water, insufficient to

cover the whole lake bed or dissolve all the

salt, enter the lake and reach the southern

bays al relatively frequent totervals of 1 to

10 years. Major floodings, covering the lake

bed completely and. dissolving all the salt crust.

would appear to occur at widely separated in-

tervals of the order of 30 years (Bonython &

Mason 1953). This occurred in 1949-50 and

was well documented (Bonython & Mason

1953; Bonython 1955; Mason 1955),

Observations and investigations of the salt

crust in Madigan Gulf were first made by

Mudigan (1930) and later by Bonython

(1956) and the Geological Survey of the

South Australign Department of Mines (Johns

1963), In 1963 Bonython compiled on

isopachyles map of salt crust thickness in

Madigan Gulf (pers, comm,, C. W. Bonython,

Adelaide, S.A), By 1963 reasonably compre-

hensive information had been recorded about

ihe occurrence of salt in Madigan Gulf. The

existence of salt crust in Belt and Jackboot

Bays had been noted (Bonython 1956; Johns

1963) but no quantitative dala bad been re-

corded about its thickness or extent.

In 1972-73 the present authur, assisicd and

accombunied by his wife on all occasions,

carried out surveys of the distribution of salt

crust and variation in its thickness in Belt and

+ Department of Geolozy and Geophysics, Universiry of Sydney, N.S'W. 2006.

136

Sackhont Ba\s. and like bed conditions were

investigated between shorelines and crusts, and

between crusts and northern red-clay muds,

Surveys Were also carried out in Madigan Gulf

to investigale Jake bel conditions along thy

northern limits of sall erust, and also to obtain

evidence of any changes in salt disiribution

which may have accurred since measurements

were flrxt made in 1929. Results af these sur-

veys and invesligations ale presented here.

Lake Bed Surveys

Conditions on the so-called “dry” lake hed,

or lake bed withoat water cover, vary widely

from place to place, Damp or wet marginal

muds along southern shorelines jie asually

sufficiently firm to walk an, but boggy for con-

ventional and four-wheel drive motnr vehicles,

and m places too soft for motor bicycles with

normal-width tyres. Salt crusts in the southern

bays overlie slushy mud. The atrength of the

erust varics from place in place, depending

Inrgely on bulk densiiy. In general, however,

crusts less than 2.$ cm om thickness may not

support persons Gn foot er motor bicyeles, and

anything breaking throueh will sink inte under-

ying Mush. Crust aver 10 cm in thickness

will support light vehicles and those over 20

em will support heavier vehiries such js

medium-weight trucks,

To curry out comprehensive surveys on the

luke hed, ir wiis necessary to have a meuns of

transport for persons and equipment which

would trayel over as wide a range of surtace

conditions as possible, at speeds up to ahoul

4f) km.p.h. Honda “ATC 90" motor tricycles,

Weiehing about 90 kg cach and eanipped with

bulloon tyres 34 cm Wile and 68 emi in

diameter, were successfully used, These

michines, tawing light equipment trailers,

would each carry ane person over surlaces an

which it was not possible to walk, When they

broke throush into watery slush the buoyancy

of the three balloon tyres Kept the machines

afloat and facilituted recovery fram otherwise

hopelessly bogeed conditions

Maps used for the surveys were based on

the 1:250,000 topographical sheet SH53-4 Ed,

|. Series R502, prepared by the Common-

wealth Division of National Mapping from

aerial phategraphy, Aerial photoanosaics pre-

pared) by the South Australian Department of

Lands were also used for mapping and photo-

interpretation in the investigation of lake bed

conditions. Distances on the lake bed were

measured by cyclometers attached! to the

wheels of the tricyeles. Magnetic bearings were

J, A, DULHUNTY

tsliblished by surveying compasses, and lines

along bearings were marked by black flags at

intervals of 1 mile (1.609 km), Sult thickness

was determined hy horing an 8 mm dianreter

hole through the crust, with an auger and

brace, then inserting a mictut rod with a right

aigle hook at its end, hooking the base of the

crust, and meastiting its thickness. Where salt

crust was absent, or less than 1 em in thick-

ness. the condition of the lake bed was assessed

as “vompetent® where it would support a

standing person, or ag “incompetent where a

person attempting to stand would sink into

Nuid mud or watery silt.

Before commencing lake bed surveys, broad

roconnaissances were curried Out over the three

southern hiys of the lake, and for 24 km north

werosy the centre of the luke rom Hambidge

Point. Survey lines, most likely to yield

significant data, were first selected on the map

across Madigan Gulf, Jackboot Bay and Helt

Bay. The selected survey lines were then estab-

Jished on the lake. and salt crust thicknesses

woud lake bed conditions were measured and

assessed at numerous points along each line.

After consideration of results, additional lines

and points were sclected for further surveys. Tn

some places levelling was carried out along

survey lines. as the first part of a comprehen-

sive level survey, us yet incomplete. Acrial

photo-interpretution, based on ground control

established during ‘uke bed surveys, was

carried out and followed by a law. ji Ntitude

aerial reconmatssance,

Results and Conclusions

Results of surveys and investigations of the

lake bed are Wustewted in Fig. 1. Thickuesses

ol salt along survey lines, and at isalied

points, are shown in centimetres at points of

measurement. Many more mensiremenls were

made along survey lines than could be shown

in Fig. 1. Atcas of conypetent mud ure shown

between shorelines and salt crust sheets m the

three southern hays. Areas of incompetent

sill or slush are shown extending east and

west across the Inke between the southern salt

sheels und the ted clay suriace to the north

Salt Crusts of Jackhoet and Belr Bays

Well developed salt crusts were found in

both Jackboot and Belt Bays. ‘The thickness

and extent of salt in cach bay at the time of

the survey during the winter of 1972, is iu-

strated in Fig. 1, The crusts were separated

from the shere bv zones of shoreline nial,

from 0,1-2 km wide, which were moist and

127

LAKE EYRE NORTH

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soil, sumewhal aandy, mostly competent to

walk on bul bogey to motor vehicles. Salt

crust Was Cominuous cound the northern en

of Babbage Pepinsula, The greatest thicknesses

of sale measured were 29 cm in Belt Bay and

23 em in Jackhaot Bay. In both bays the maxi-

muni thickness of salr occurred close to, and

about midway along, their eastern shores.

Tn centra) aveas of the salt sheets, thickness

changes were mostly very gradual, but at some

plates wuddun chunges occurred, Along a hear-

ina of 307° magnetic from Bonython Head to

the morthwest head of Belt Bay (Fig. 1). salt

crus (hickness decreased gradually From 29

em near Honython Head to 20 em near the

centre OF rhe bay, over a distance of 10 km,

Then it decreased suddenly to 10 env over

approximately 1.5 km {between the thickness

points af Zl) and LO cm shown in Fig. 1),

following which it increased gradually to 13

em, then remained between 12-13 em for 5

km, and finally thinned rapidly, as usual, near

the shoreline. A level survey along the same

line across the eentre of the bay showed a

gritual uniform rise on the upper surface of

the sall, indicating that the sudden thickness

chanyves were stepdike undulation in the lake

bed yt the base of the crust. Simifac, but less

pronounced evidence of sub-critsiq] steps in

the lake bed was found in Jackboot Bav and

Miatigun Gute The lower portions of the salt

crust, present in 1973, had probably formed

during 1952 by evaporwtion of the 1949-30

flood Waters, and remuined tnattected by suh-

sequent minor fillings which dissolved and

redeposited only ihe upper pertians af the sali

chust, From this it would seen likely thar the

sleptike tindulalions were Tormed by scouring

of ehinnely or areas in the lake bed after solu-

lion of the Whule erust in 1950 aod 1951. anc

before its subsequent redepositian in L452.

Yhe Slush Zone

To the north of Jackboot and Bele Bays

between Hunt Peninsula and the western shore.

and in the northern areas of Madigan Gulf

between Hunt Peninsula and the eastern shore,

salt crusts (hin out a5 they pass to the north,

and unsterlying silt; consist of incompetent

slush. In these areas salt crusts ure of low

strength, Light motor vehicles and heuvy ani-

male such as camel break through crusts af

7-8 em) persons on foot or conventional motor

cycles break through crusts of 2-5 om, and

motor tricycles with balloon tyres, as used in

the present surveys, break through ecmists of

1-3 em, Anything breaking through the thin

J, A, BULHUNTY

erust sinks Into underlying slush und becomes

bogged, Wild cumels, which had broken

through 7 cm of salt, were found 3 km east of

Hunt Peninsula m the north-western area of

Madigan Gulf They had foundered or

strugvled for ouly ¥ om before dying of exh.

tion earlier in 1972, to be entombed in Recent

sediments and preserved as future fossils under

conditions similur to these which trapped and

preserved the now extinct diprotodans whose

remains are found in Pleistucene sediments

around Lake Eyre (Surton, Tedford & Miller

1961). Persons sinking into the slush can

neither swim nor wade, and must crawl or

roll over crumbling salt and mud to. reach

crust strong enough to support their weight

when standing, In seme plices the crust is

only U.5-1 em thick, whilst in others it is little

more than an encrustation of 1 mm or less

which is dissolved und removed by epeh fall

of rain, but but up again between tainfalls

hy evaporation uf brine rising through the sill.

Aveas described above are the most treach-

erous and difficult to negotiate tn the whole

of Lake Eyre. As far as could be ascertained

from surface exploration amd aerial photo-

interpretation, che arcas extend right across

the lake for about 65. km, on an east-west

whgament through the north head of Hunt

Peninsula. They form 4 zone from about 7-12

km wie. for which the term “Slush Zone’ hs

proposed, as tlustrated in Fig. 1. It encloses

practically all of Brooks Island. the narth head

of Hunt Peninsula incliding Hambidge and

Artemia Points, and a large island siltated 11

km west of Hunt Peninsula. M1 is almost impas-

sible to Uravel into the Slush Zone over the

surface of the Inke bed, Prior lo the present

survey, Ike only party ta reach Braoks Island

truvelled hy boat during the 1449-50 flood

(Bonython 1455, p. 27), During the investiga-

lions of surface cunditians in 1972, the Juke

bed trom Hunt Peninsula to Brooks Island was

crossed hy Honda motor tricycles. travelling

over 1-2 em of crust in the Slush Zone. The

crossing was penlous intl succeeded only by

travelling at a speed of xhoul 35 kmep.h.. as ut

lower speeds the muachines would have sunk

into the slush, A similur utlemipt to travel over

the lake bed to the large tsland west of Hunt

Peninsula was nmsuecessful as the machines

and riders broke through a crust of 1 ent or

less und sank into the underlying slush, How-

ever it wax teached by boat during a minor

figading of Belr Bay in July 1973, which made

possible an cswmination of the island and lake

LAKE EYRE NORTH

bed in the western Slush Zone. A perminent

survey mirk, consisting of 1.5 m of copper

pipe driven 0.75 im into the ground, was left

at at) elevated place, situated 640 m in a direc-

tion 325° magnetic from the most southern

point af rhe island, As far as is known this

was the first occasion on Which anyone had

Teiched the island,

Hambidge Paint

The Slush Zone, situated a little south of the

geagriphical centre of the lake, forms a barrier

to worth-seuth Iravel on its bed, There is only

one place at which, if condilions are suitable,

it can be crossed hy persons on foot or on

conventional motor vycles. This is from the

northern shoteline of Hunt Peninsula, where

sand has been carried out into the Slush Zone

by south-east to south-west winds. Bonython

crossed the Slush Zone from the tip of Ham-

bndge Puine in 1970, ond walked for some 20

kin to a point bearing 348° magnetic fram

Rambidue Point. which he calewated as close

fo the geographical centre of the Iake (pers.

coin. C. Warren Bonython, 1972, Adelaide,

S.A), During the present Jake hed survey,

réconnuissance was mide from a point on the

shoreline about 2 kim south-east fram) Ham-

bidve Point to true north across the Slush

Zone, for 24 km over the central region of the

lake.

Between Uambidge Point and a small island

about 1.5 km to the north, the level of the lake

bed falls slightly, by about 30 cm to a channel

long which water flows round Hunt Peninsula

when sufficient siceumulites in either Belt Bay

or Madigan Gulf to cover the lake hed as for

north as Hanibicdge Poini, The existence af

such w channel. linking Belt Bay and Madigan

Gulf, and whe possibility of water flowing along

it fram one bav to the other, was first sug-

gested by Bonython (1955, p. 8). This pru-

cess wis observed in operution during ihe

winter of 1973. Water Nawing down the War-

burton Groove filled Belt Bay afmosi to (lam-

hidue Point. When strong sowth-westerly winds

moved the water north-east, tt reached a depth

of about 15 cm at the Pont, and flowed eust

along the channel. It then spread out over a

witle srca northwest und west of Brooks

island. communicating with Madigan Gulf only

by a marrow and shallow jrea along the eastern

side of Hunt Peninsula, south from Ariemia

Point, Before finding ils way into Madigan

Gulf, inest af the water was blown hack round

Hambidze Point tito Belt Bay by south.

easterly to |orth-easterly winds, whiol usnally

follow soon after south-westerly wines

Fle Northern Reed Clay Surface

Daring the reconnyissance 74 km north

from Hambidge Point, some information was

gained about the general nature of the Jake bed

in central areas, North of the channel in the

Slush Zone round Hantbidge Point, the lake

bed gradually beeame firmer and drier, as the

wet, black, grey and preen silts of the Slush

Zone carrying a soft thm salt crust, were re-

placed by damp red or yellow-red clay. carry-

ing in places a thin soft powdery salt. but no

crust. Between 20 and 24 km noith of Ham-

bidge Point, the surface of the clay was ulmost

dry and suncracked. with thin aprurned flakes

of dry clay and very liule dry powdery salt.

A comprehensive and detailed study of the

northern half of the lake bed remains to be

accomplished: however, progressive changes to

the north in the nature of the lake bed, des-

cribed above. are in accord with the Fact that

the lake bed falls genily io the south, provid-

ing draimage info the southern bays which

serve a8 4 sump. or “xeodetic centre’, of

1.300,000 sq. km of internal drainage.

Self Crusty of Maegan Gulf

Sul erual thicknesses in Madigan Gulf,

measured during (he winter of 1972, eanfirmed

the agcurrence of i large area of sult crust as

described jn previously recorded information,

to which reference has alrendy heen made. It

wus stparuled From the shore by shoreline mud

from O.5-4 km owe. avernging about

2.5 km. A maximuny crust thickness of 46 ent,

the grewtest thickness of sult ever recorded in

Lake Eyre, was formd near the centre of Madi-

gin Gulf, and a consideruble yreqy was aver 30

em thick. as illnstrated in Fig b. WDerail sur-

veys Of sale crust thickness were carried out,

across the previously mapped and measured sale

crust of the gulf, with the objecé of detecting

changes in thickness and distribution which

may have occurred over the period nf 43 years,

from the firsy recorilet measurements to 1972.

In 1929 Madigan (1930) walked for 18,9

km tna direction 324° magnetic fram Presentt

Point to the central area of Madigan Gull,

apd measured salt thickness at 6 places along

the mute, During 1954, Bonython (1956)

carried out an cxtensive survey for 24 ken

along 305° magnetic, from Prescott Pot, ond

also G other lines across and near the central

area of the gull, measuring salt thickness at

numerous places, In 1961, the Geological Sur-

130 J, A. DULHUNTY

“pont (Looks MADIGAN GULF

I, (LAKE EYRE NORTH)

LEGEND

TRAVERSE LINE WITH NUMBERED #3

SALT-CRUST MEASUREMENT POINTS

SALT THICKNESS IN CENTIMETRES

MEASURED BY '

MADIGAN, 1929... ... M30

BONYTHON , 1954. B28

S.A, GEOL-SURVEY,|961.678'

DULHUNTY, 1972 D6"

CENTRE-POINT; INTERSECTION

OF LINES H-J,.-M,N-O cP®

CAMPBELL

POINT

oO.

Bil

Wing p23 02% De

H 1 (a

WILLOW

HEAD

SHELLY

ISLAND

FIGURE 2

LAKE EYRE NORTH 4)

yey of the South Australian Department of

Mines ¢(Johus 1963) mensured thicknesses for

ever 40 km fram Prescott Point along 305°

Magnetic, Tinally, in 1972 the present author

measured thicknesses along 305° magnetic for

44 kin from Prescott Point to the shore of

Hont Peninsula near Artemia Point. and also

along, 6 other Jines Over Madigan Gull,

Results of the foregoing salt crust thickness-

Measurements ate shown on the map of Madi-

gim Gulf in Fig. 2. Lines along which measure-

menls were made are designated by capilal

letters, Positions at which meusurements were

made along each hne are aumbered consecu-

\ively from the more southerly end of the

line. Thicknesses af é¢ach point are preceded

by letters indicating the persons who made the

measurements, as indicated in the Jegend of

Fly. 2, For example, at point 8 on line P—A,

24 cm of sult was measured by Bonython in

1954, 20 om by the Geological Survey in

1961, aiid 39 cm by Dulhunty in 1972: ay

point 4 on line P-B, Madigan measured 20 ¢m

in 1929: slong line E~G, Bonython measured

25 em at point 6 if 1954 ond Dulhunty

measured 14 cin at point 5 in 1972. Along line

P-A, measurements hy the Cieological Survey

and Dolhunty were made at Intervals of 1 mile,

wr 1.609 km, as shown in Hig, 2, Measure-

ments by Banython (7956) were noe all at 1

nite Intervals, and a small amount of inter-

polation was necessary in transferring his

results lo jhe intervals shown along linc P-A in

Fig, 2 Ti ath other cases, thicknesses ote

shown at the points measured hy the persons

concerned.

Some interesting facts, problems and con-

cliisiois emerge From the data assembled fn

Fig, 2:

I, Sali crust measurements by Madigan, along

line P-B jn 1929, show 18 em at 3 km fram

Prescott Point, 00 Crist at point 2 on Kunoth

Shoal, and an increase in thickness from 9 em

at point 3 to a maximum of 43 em at point 6,

the lini mM his traverse. The rate of increase

falls off between poiits 5 and 6, indicating the

cxistence in 1929 of an appreciable area, per-

haps 4 km in diameter, with a crust. thickness

of at least 40 em. This crust, which may be

referred io as the “Madigan Crust’, hed been

m cxisteiice for sume years before Madigan

Treasured it in 1929. Tt must have originared

by redeposition of sall during the drying up

of the gulf after an early, unrecorded major

filling which had dissolved the whole uf the

pre-existing crist, The Madigan Crust, so

formed, suryived partial <ohition and redeposi-

tion during iminer Aloodings, antil the nexl

major fillmg in 1949-50 when it was com-

pletely dissafved (Bonyihon & Mason 1953,

Bonyithon 1955, 1956).A new erust, which

could well be called the “Bonython Crust" was

then formed by redeposition af salt as the

gulf dried up during 1952,

In 1954, when the Bonython Crust was only

2 years old, Bonython measured thicknesses of

28 umd 29 cm at points 2 and 3 on ling D-E

(Vig. 2) near the centre of the gulf, close 10

where the Madigan Crust hat been 43 cm in

1929, When the Bonython Crust was 20 yeurs

old, in 1972, Dulhunty measured 4046 cm

of sall in the central are where it had been

28-29 cm in 1954. From this it is evident hat

the crusts of Madigan Gulf change in thick-

hess with lime, following vomplete solution

and redeposition (Bonython 1956), Within an

ate of about 16 sq. km, near the cenlre of

the gulf, the Madigan Crust had reached a

thickness of 40-43 cm by 1929) the new Bonv-

thon Crust was 28-29 em thick whet 2 yeiurs

old in 1954, and 40-46 ens thick when 20

years old in 1972. If the increase to a thick-

nese of 40-46 cm in 20 years is representative,

Or approsimates to normal rate of change in

the central area of the pulf, then it could be

suggested that the ofd Madigan Crust was of

the order of 20 years old whon measured hy

Madiean in 1929. Careful shudies of rainfall

Tecords ¢Bonvihon & Mason 1953; Mason

1955, p, 11) from 1880 to J943. compared

with rainfills for 1949-30 which produced a

myer filling and completcly dissolved the

crust, sugzest possible floodings in 1887-88,

1890-91, 1906-07, 1917-18 and 1920-21.

Water could have entered the lake on these

occasions. but nor alwavs in suflicient quantity

to Gill it and dissolve the whole crust, If the

Madigan Crust was 20 years old, and no more,

in 1929. then it would have been the hish-

rainfall year in 1906-07 that Iced to major

filling with sulution of the pre-existing crust.

Jt is possible, however, that crusts of Madigan

Gulf may incresse in thickness {a beiween

40-46 cm over 20 years, and then remaia

more or Jess constant, In this case, the earlier

high-rainfall year of 18M91, regarded by

Bonython (1953) as the most likely to have

prodticed a major filling. could have led to the

deposition of the Madigan Crust 36 years

before Madigan measured it.

Tn general, thé present evidence and car

clusions based on studies of chanpes in salt

132

32 J, A. DULHUNIY

erust thickness with lime, support previowis

Opinions (Bonython & Mason 1953; Mason

1955, p. 11) that Lake Eyre hud heen filled

to cover its whole bed and dissolye the whole

crust ha more than twice in the last 90 yeirs,

approximating perhaps to an event which

huppeas twice a century under existing en-

vironmental condilions.

2 The crist thicknesses shown along line

P-A, front peints 1 to 15, were measured by

Bonython, the Geological Survey and Dul-

hunty when the Bouython Crust was 2, 9 and

2) years old, respectively, From pommts 16 to

23, measurements were made at 9 years by the

Geological Survey and 20 years by Dulhunty,

and from puintis 24 to 26 at 20 years by Dul-

hunty only, The line P—A, bearing 305° mag-

netic, extends across the gulf somewhat to the

south-west at the central area.

From points 1 to 15 along linc P—A, thick-

ness figures show a general thinning of the

crust for 7 years after if was 2 Years old. Then

iL increased im thickness over the next 11 years,

to 20 years old, Similar thickening also

occurred further along the line between points

15 and 23. Although amounts of thinning and

thickening were somewhat irregular, in

general early thinning was greater in more

marginal areas but catended right peross the

more centri area, and later thickening was

greater in the more central area but extended

well into marginal areas. The genctal principle

of transfer of sale from higher marginal areas

to lower central areas with time (Bonython

1956) oo doube operated throughoul the his-

tory of the crust, but some other factors must

Nave caused ently thinning ucraxs the more

central area, and extension of Iater thickening

well into maryvinal aureus. Such factors, as vet

unknown, bul possibly associated with lake

bed instability, could have inffuenced the direc-

tion of gradionts on the surface of the crust,

changing dircetions of water dramage and salt

transfer.

3. In 1954, Bonython (195h) measured sall

crust thicknesses ul points, 2. 3, 4 and 5 along

line D-E bearing 35° magnetic, and also at

points 3 and 6 along tine E-G bearing 305°

magnctic. Line D-E traversed the central! rea

of the gulf and line E-G trended north-

westerly away from the centre as pllustrated in

Fig, 2, The crust was of very uniform thick-

ness of abour 28 cm. with one point at 27 cm

unil aimother at 29 em ut points 3 und 4 on

line DHE

At the intersection of lines M-L and D-E,

Dulhunty in [972 measured 41 cay of sult

where Bonyihon hud found 28 cm in 1954

About 6 km north-easterly, at the intersection

of lines BD-E wad E-G, the crust was 31 cm in

1972 und 28 cm in 1954, and in the vicinity

af points 2 and 3 on line EG thickness fell

to 25 cm where it had been 28 env in 1954.

Further north-westerly along Jineé E-G near

points 5S and 6, where Bonython (1956) had

recorded his Lowest level in Madigan Gulf, the

crast wis only 19 em in 1972 compared with

28 em in 1954.

From the foregoing data, at is evident that.

between 1954 and 1972, salt crust thickness

had increased hy 13 cm near point 2? on line

D-E jn the central area, remained constant

between points 1 and 2 on line E-G 7 km

north-easterly, and decreased by 9 cm near

pointy 5 and & on line E-G 6 km north-

westorly, This would appear to mean that an

appreciuble transter of salt had taken place

jn 18 yours, from north to south, from Rony-

then’s lowest plaice towards the centre of the

gull over 4 distance of 10 km. As shown by

Bonython’s level fieures (1956) the surface of

{Ive lake bed. at the base of the crust, in 1954

glaped down generally to the north, fram point

2? on D-E to point 6 on B-G, by un amount

of (0.32 m ¢1,.7 fL)- The salt eruse in this

vicinity varied only between 28 and 29 cm,

so its upper surfyce must have sloped generally

north at ubout the same gradient. Therefore

the teumsfer of salt from narth to south

between 1954 and 1972, although from more

marginal fo central) areas, would appear te

have been “up hill” over a gradicnt averaging

5,2 cm per km. The normal transfer of salt

with time. described by Banvthon (1956),

tukes place actoss surfaces sloping down from

marginal to central pres, aver which water

carrying sall im solution flows to deposit salt

on drying in Jower areas,

tt would seem that transter of salt from

north to south, across the area described

ahove, could have been made possible only by

some change in levels of the lake bed over

the period concerned. This and other prob-

lems of relations between salt distribution and

tevels of the lake bed warrant further research

beyond the scope of this paper. As a result of

the present investigations, it is believed that

changes with time in relative levels of differcot

parts of the lake bed should at least be con-

sidered possible, until the Occurrence of any

stich phenameng fas been mon: definitely

LAKE EYRE NORTH 133

established and its nature and causes are more

clearly understood.

Acknowledgements

It is wished to acknowledge (i) co-operation

and assistance generously provided by

Muloorina Station, without which field investi-

gations would not have been possible, (ii)

valuable discussion with C. Warren Bonython

of Adelaide, members of the Department of

Geology, University of Adelaide, and the Geo-

logical Survey of South Australia, and (iii)

provision of research facilities and field equip-

ment by the Department of Geology and Geo-

physics, University of Sydney.

References

Bonyruon, C. W, (1955),—Jn “Lake Eyre, South

Australia, The Great Flooding of 1949-1950".

The Report of the Lake Eyre Committee, R.

geogr. Soc, Aust. (S. Aust. Branch), pp, 7-9,

27-56, 63-70. (Griffin Press: Adelaide.)

Bonytiton, C, W, (1956).—The Salt of Lake

EByre—Its occurrence in Madigan Gulf and

its possible origin. Trans. R. Soc. S. Aust,

79, 66-92, pl. 1-8.

Bonytuon, C. W. (1960).—A decade of watching

for water in Lake Eyre. Proc. R. geogr. Soc,

Aust, (S. Aust. Branch), 61, 2-8.

BonytHon, C. W., & Mason, B. (1953).—The

fillmg and drying of Lake Eyre. Geogr. J.

119 (3), 321-330.

Jonns, R. K. (1963).—Investigation of Lake

Eyre. Pt. 1. Rept. Invest., geal. Surv. S.

Aust. 24, 1-41.

Manican, C. T, (1930).—Lake Eyre, South Aus-

tralia. Geogr, J. 76 (3), 215-240.

Mason, B. (1955).—in “Lake Eyre, South Aus-

tralia. The Great Flooding of 1949-1950”.

The Report of the Lake Eyre Committee, R.

geogr. Soc. Aust. (S. Aust. Branch), pp. 11-

26, (Griffin Press: Adclaide.)

Srirton, R, A,, TEpForp, R. H., & MILLER, A. H.

(1961).—Cenozoic stratigraphy and verte-

brate palueontology of the Tirari Desert,

South Australia. Rec. S. Aust. Mus. 14 (1),

-61,

Wiuuams, A. F. (1973)—LAKE EYRE Map

Sheet and Explanatory Notes, Geological

Atlas of South Australia, 1:250,000 series.

(Geol, Sury. S. Aust.: Adelaide.)

Worener, H., & Twmace, C. R. (1967).—Geo-

morphological history of the Lake Eyre

Basin. In J. N. Jennings & J. A. Mabbutt.

Eds., “Landform studies from Australia and

New Guinea”, pp. 118-143. (A.N.U. Press:

Canberra.)

THE GENUS POTOROSTRONGYLUS JOHNSTON AND MAWSON

(NEMATODA: TRICHONEMATIDAE) FROM MACROPOD MARSUPIALS

BY PATRICIA M. MAWSON*

Summary

MAWSON, Patricia M. (1974).-The genus Potorostrongylus Johnston and Mawson

(Nematoda: Trichonematidae) from macropod marsupials. Trans. R. Soc. S$. Aust. 98(3), 135-137,

31 August, 1974.

The genus Potorostrongylus is redefined, and it is suggested that it is most closely related to the

genera Zoniolaimus and Labiostrongylus. P. finlaysoni, the genotype, is recorded with additional

details of morphology from Potorous apicalis and Bettongia gaimardi from Tasmania.

P. aepyprymnus n.sp. is described from Aepyprymnus rufescens from Queensland.

THE GENUS POTOROSTRONGYLUS JOHNSTON AND MAWSON

(NEMATODA: TRICHONEMATIDAE) FROM MACROPOD MARSUPIALS

by Parercia M. Mawson*

Summary

Mawson, Patricia M- (1974),-—The genus Poterostrongylus Johnston and Mawson (Nemua-

toda: Trichonematidac) from macropod marsupials. Trans. R. Soc. S, Aust. 98 (3),

135-137, 31 August, 1974.

The genus Potorostrongylus is redefined, and it is suggested that it is most closely related

to the geaeta Zoniolaimus and Labiostroneylus. P. finlaysoni, the genotype, is recorded with

additional details of morphology from Poterous apicalis and Bettongia gaimardi from ‘Tas-

mania. P. aepyprymaus nsp. is described from Acpyprymnus rufescers from Queensland.

Introduction

The genus Potorostrongylus Johnsion &

Mawson (1939, p, 306) was placed by Yama-

gut? (1960, p, 403) as a subgenus of Zenio-

laimus Cobb, and by Popova (1960, p. 220)

among genera insufficiently known; Chabaud

(1965) did not mention it,

New material is now available, including the

type species P. finlaysoni Johnston & Mawson

from the type host from a new locality, as

well as specimens from a different host and

locality, apparently representing a new species.

It appears that Zoniolaimust Cobb (1898.

p. 312), Labiostrongylus Yorke & Maplestone

(1926, p. 67) and Potorostrongylus have many

features in common, Petorosirongylus is dis-

tinguished from Labiostrongylus mainly by the

shape of the oesophagus and the tvpe of

papillae on the genital cone, and from Zonio-

Jaimus by these features and by the very small

buccal capsule, A revised diagnosis is given:

Trichonematidae: Zoniolaimimae: Cervical

cuticle inflated; anterior end with cight well

developed lips, four submedian cephalic

papillae and two lateral amphids on cor-

responding labia, dorsal and yentral labia with-

out papillae. Short cylindrical cuticular buccal

capsule; oesophagus cylindrical, ending in a

consitiction follawed by elongate bulb, Male:

spicules equal; bursa only slightly lobed; dorsal

tay bifid. each branch giving off a short lateral

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

stem, externo-dorsal ray arising separately;

yentro-lateral separate for most of its length;

the ventral genital cone well developed, bear-

ing a row of stout setae on ventral lip of

cloaca, and two small cuticular alae Jaterally.

Female; vulva shortly in front of anus, vagina

short, ovyejectors Opposed, uteri both anterior

to vulva,

Parasitic im” stomach of macropod mar-

supials.

Type species: P. fnlaysoni Johnston & Maw-

son,

Other species: P. aepyprymnus 1.5p-

Potorostrongylus finlaysoni Johnstan & Maw-

son, 1939: 308, From Potoreus gpiculis

(Syn. P. midactylus), from Gippstaiid, Vie.

FIGS. 1-6

Hosts und localities: Pororous apieuiixs, Betion-

gia gaimardi, from Tas.

The new specimens agree with the earlier

descriptions in most features. but some addi-

tional points have been noted. The length of

the new, uncontracted, specimens is up to 13

mm in the male, to 15 mm im the female. The

cuticular swelling at the anterior end is usually

confined to the region from just behind the lips

1 about a third or balf the length of the

oesophagus. At the anterior end of thts swell-

ing there is a ting of refractile bodies in the

cuticle: this probably has a strengthening

1 Zoniolaimus is considered as having the characters of the lype species Z. svtifere Cobb; some species

with “teeth” have been wrongly attributed to this genus.

136 P. M. MAWSON

Figs. 1- 6. Potorostrongylus finlaysoni. Fig. 1—Qesophageal region. Fig, 2.—-Head of female, dorsal

view. Fig, 3—Head of female, en face; t = thickening in cuticle. Fig. 4——Dorsal ray.

Fig. 5.—Genital cone, ventral view. Fig. 6.—Tail of female.

Figs. 7-12, P. depyprymnus, Fig. 7—Head of male. Fig. 8.—Oesophageal region. Fig. 9.—Bursa. Fig.

10.—Dorsal ray. Fig. 11—Genital cone, lateral view. Fig, 12.—Tail of female,

POTOROSTRONGYLUS FROM MACROPFOD MARSUPIALS \37

effect. The eight lips also are strengthened,

each having a V-shaped thickening of the

cuticle just inside the free margin (Fig. 3, 1).

No papillae have been seen on the dorsal and

ventral lips, which are mostly cuticular

thickenings, with very little pulp. The shallow

buecal capsule is faintly striated, and its. an-

lerior gnd is turned outwards (Fig. 2), The

lining of the oesophagus is strongly cuti-

cularised at the angles of the triradiate lumen,

giving the appearance of three longitudinal

rods uown the length of the ocsophagus. These

toads are particularly thick in the terminal bulb,

und are interrupted at its midlength. The seti-

form cervical papillae lie at about the Ievel of.

of just behind, the excretory pore.

The bursa and bursal rays apree with the

originil description. The genital cone is well

developed, and bears .a small ala on euch side,

as, Well as about 12-13 cuticular projections

forming a fringe along the ventral lip of the

cloaca,

The tail of the female is long and slender,

tapering to y blunt tip; the vulva is about twice

the tail length from the posterior end of the

body.

Poterostrongylus aepyprymuous i..sp.

FIGS, 7-12

Host and locality: Aepyprymmlus rifercens,

from Warwick, Qld,

‘The general morphology of the specimens

from Queensland is very similar to that des-

cribed for P. finfaysoni. The ditierences are:

P. aepyprymnus is a smaller worm; the dips

ate shorter, so that the buccal capsule lies

behind the lips instead of, as in P. fitleysont,

at the level of the Jower half of the Jip region,

The oesophageal bulb of P. aepyprymaus is

much more elongate than that of P. jfinlayseni

and the break in the cuticular lining js al two-

thirds of its length.

The bursal rays are similar except for the

dorsal ray, of which the lateral branches are

distinctly longer; the génital cone is similar in

shape and bears a precloacal row of about 12

setae as Well as a pair of Jateral alae which are

however situated slightly more posteriorty on

the cone than those of P, firlaysoni. The spi-

cules are slightly shorter in P. aepypryninns,

The tail of the female is shorter and rela-

tively thicker than that of P. finlaysont. Na

eggs are present.

Measurements are given in Table 1,

TABLE |!

Mevisurements of P. aepyprymnos. All mreosure-

ments are in wun,

a 4

Length 5200-8000 5010-5500

Desophagus 830-950 820-900

Antr, end—nerve) ring 350-420 310-350

—tervical pap. 470-600 390-440)

—excr. pore 460-580 380-490

Spicules 960-1050 -

“Tail : . 70-200)

Vulva-—postr. end - 350-450

Body leheth/oesoph, leieth 5.4-7.6

Body lengib/spicule Jength 6,2-8.4

Acknowledgements

The specimens from Tasmania were

obtained through the kindness of Dr. J, Hick-

min of the Zoology Department, University

ot Tasmania, and Dr. B; Munday of the Tas-

manian Department of Agriculture, Launces-

ton. The single specimen of Acpyprynmus

rufescens was obtained through the courtesy

of the South Australian Museum, I am most

gratelul for this help.

References

CHavaun, A, G (1965).—Ordre des Strougylidu.

In Pierre-P.Grassé. (Ed.j), “Traite de Zoo-

Jogie”. Vol. 4, pp. 869-931. (Masson et Cie:

Paris.

Conk, N. A, (1898),—Extract from M.S. Report

on Parasites of Stock. Agric. Gaz. N.S. 9.

296-321,

JounsTon, T, H. & Mawson, PL M. (1939).—

Some nematodes. from Victorian and Westerti

Australian marsupials, Trans R, Sec §. Aust.

63, 307-310.

Popova, T. ft, (1960),—‘Principles of Nema-

todology.” Vol. 9, Cloacinidde. (Moscow

Acad, Sci, USSR.) (In Russian.)

Yasamuti, S. (7961).—Systema Helminthum.”

Vol, 3, ‘The nematodes of vertebrates. (Inter-

science: New York.)

Yorks, W. & MAriestone, P, A. (1926)—"The

nemalode Parasites of vertebrates.”

(Churchill; London.)

THE CORROBINNIE DEPRESSION, EYRE PENINSULA,

SOUTH AUSTRALIA

BY JENNIFER A. BOURNE*, C. R. TWINDALE* AND DIANE M. SMITH*

Summary

BOURNE, Jennifer A., TWIDALE, C. R., & SMITH, Dianne M. (1974).-

The Corrobinnie Depression, Eyre Peninsula, South Australia. Trans. R. Soc. S. Aust. 98 (3),

139-152, 31 August, 1974.

The Corrobinnie Depression is a narrow, elongate, essentially linear feature which trends NW-SE

across northern Eyre Peninsula, South Australia. It is characterised by the presence of numerous

salinas and parabolic dune fields, which stand in contrast to the linear sand ridges of the adjacent,

higher plains. The Depression is certainly a structural feature, though its precise origin remains

obscure. It could be a fault-line valley eroded by rivers, the outlet of which can no longer be

detected, or it could have originated as a fault-line depression due to the weathering of the rocks in

and adjacent to a fracture zone by groundwaters, or by volume decrease of the weathered rocks and

consequent subsidence of the land surface. The Depression dates back to at least the early Tertiary,

and its advanced development is due to its proximity to the upstanding Gawler Ranges which shed

water to the fracture zone, thus causing it to be weathered and lowered to a much greater degree

than other fracture zones in the vicinity.

THE CORROBINNIE DEPRESSION, EYRE PENINSULA,

SOUTH AUSTRALIA

by JENNIFER A. Bourne”, C. R. TwinaLe* and DIANNE M. SmitH*

Summary

Bavimne, Jonnifer A., ‘T'wipaie, C. R.. & Smut, Dianne M. (1974).—The Corrobinnie Depres-

sion, Ryre Peninsula, South Australin_ Trans. R. Soe, S, Aust. 98 (3), 139-152, 31 August,

1974,

The Corrobinnie Depression is a narrow, clonzgatc, essentially linear feature which trends

NW-SE across northern Eyre Peninsula, South Australia. It is characterised by the presence

of numerous salinas and parabolic dune fields which stand in contrast to the linear sand

ridges of the adjacent, higher plains, The Depression is certainly a structural feature, though

its precise origin remains obscure. It could be a fault-line valley eroded by rivers, the outlet

of which can no longer be detected, or it could have originated as a fault-line depression due

to the weathering of the rucks in and adjacent to a fracture zone by groundwaters. or by

volume decrease of the weathered rocks and consequent subsidence of the land surface, The

Depression dates buck to at least the early Tertiary, and its advanced development is due to

its proximity to the upstanding Gawler Ranges which shed water to the fracture zone, Lhus

causing it to be weathered and lowered to a much greater degree than other fracture zones in

the vicinity

Introduction

Following a geological exploration of north-

west Eyre Peninsula, Jack (1912, p. 19)

reported a “depression between the granitic

ridge, the peaks of which ars visible from

Wallala Rock te Weedina” (i.c, Mt. Wudinna)

“and the Gawler Ranges . . . ". This depres-

sion, which has beett called the Corrobinnie

Depression after the prominent granite insel-

berg which lics within the lowland, extends

unbroken from the vicinity of Balumbah, 12-

13 km south-west of Kimba (Fig. 1) to the

neighbourhood of Toondulya Bluff, 200 km

to the north-west.

The Corrobinnie Depression is most readily

discernible on topographic maps or air phato-

mosdics where it is scen to form an elongate,

natrow zone of complex but dominantly para-

bolic dunes which carry a thick and virtually

undisturbed cover of cucalypt and acacia

scrub, These arcuate dunes stand in slrong

contrast to the fields of regular NW-SE trend-

ing longitudinal dunes which occur on the

slightly higher ground to either side of the

Depression. Despite its shallowness—it stands

only 35-40 mi below the level ol the adjacent

plains—the Depression is also readily deiccted

on the ground, for there is a pronounced

descent into it from both north and south

(Figs. 2 and 8). Morcover the varied dune

orientation within the Depression makes travel

within the area difficult: more than 70 years

before Jack noted and very brietly described

the Depression, E. J. Eyre and his companions

must have traversed it while crossing from

Streaky Bay to Baxter Range for they camped

at Mt. Sturt which lies close io the northern

margin of the feature. Eyre did not specifically

record having noted a depression, which is

scarcely surprising in view of its shallowness

and the other problems with which he had to

contend, but “the steep sandy ridges and dense

eucalypt scrub” which together caused heavy

going certainly made an impression, as Eyre’s

journal entry for 21 September, 1839, cleariy

shows (Eyre 1845). A few years later J. C.

Darke crossed the Depression from Mt,

Whdinna to the southern base of Mt, Sturt

and the difficulties he and his companions en-

countcred in the way of swampy salinas and

deep sands can be gauged from the fact that

they took more than three days to travel the

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

JENNIFER A. BOURNE, C. R. TWIDALE AND DIANNE M. SMITH

140

‘wlep play pue sydvsdojoyd wwe ularly UMeICE ‘Play ang MmsiayeMy ayi—saunp sipoquied Jo pjsy ay put seurms snol3swuNU :

aut Aq paysimFunsip st yay worssaadaq, aruMtqol0D ayi O} Jusoefpe pur UsYTIM SLUJOjpur] JoleuT pue 7x2} ay} Ul OF Parajor suopesOT ‘7 ‘TL

PLER AWS IOON WENN c

ee wo Eas = OS wag

Se ime s. S

a ee 2 suis sidwes pues >

JINIMVAT seujuazida ayenbyves &

Me <a §aJ0Q 7

7. a

. FSNiava SeulES

Nic ee kee vo iN seunp

~->*—— “TMH ‘

a == a ‘

_ owsoe yeas © ars xX Soneniat 7

2s a. soi

Wer aesoaaas > =

NT on SSS

in Tes ~e

~ mn > -s Rare aganiog) >= ~~ <a _ by (

a ee ~~, Wik Ban TH es " ~ pra< S, es Th ad av

poasi¥one , = - iM Stet 9 ye “We mite SA, re

= ea Nae ‘ : : 2

Wines ind

a) x

~ 3 HDogajwong 4 '

= ‘

~ ee oe ”

Man 0

> june en,

THE CORROBINNIE DEPRESSION i4l

sal eo,

WETHES 2000® A Lotduowe |

BE:

2 = — = PT 3 a

AILOMETAES thpvigad

Fig. 2. Topographic sections between A and Ay

wad Band B; (on Fig. 1) across the Cor-

rdbemnie Depression, Drawn fram field

ata,

32 kn between the two points (S.A. Register.

13 November, 1844; Twidale 1974).

Thus though not 4 spectacular topographic

form, the Corrohinni¢ Depression constitutes

a distinet and, by virtue of its extent. a major

geomorphological feature cutting diagonally

across the broad northern base of Eyre Penin-

sulla,

What is the reason for the Depression anu

ils distinctive assemblage of landforms?

Origin of the Depression

Structural considerations, Both the extent and

lincarity of the Correbinnie Depression suggest

a structural, and in particular, a faull-generared

origin. No other explanation can satisfactorily

account tor these characteristics in combina-

tion: few fvcks older than Quaternary are

exposed in the Depression and no faults have

been observed, but # number of lines of evi-

dence and argument support the general in-

ference that the topographic feature is related

to fractures. in the crust,

Geophysical surveys, for example, suggest

that the Depression in general terms is aligned

parallel to dykes and sills which traverse

northern Eyre Peninsula and adjacent areas in

a NW-SE direction (Boyd 1970!'). Several

of these vccur within the Depression though

they have been detected only on veromagnetic

surveys. tl is reasonable to suppase that their

trend reflects weaknesses or fractures in the

erust, and similar possible fracture zohes bave

heen located in the areas south-east of Byre

Peninsula where they evidently play an impor-

tart part in delineating and determining major

telief features (see Twidale 1971, pp. 144—

149). Such a NW-SE trend is indeed an im-

portant feature of the structural pattern of the

entire Australian continent (Hills 1946, 1955),

Vhere is also some slight evidence ot seis-

micity within the suggested fracture zone. for

lwo earthquake cpicentres (Fig. 1) have been

recorded atong its trend in recent years (Sutton

& White 1968; Sutton, pers. comm.). Many

more have been recotded near the cast coast,

and to a Jesser degree the west coasl, of Eyre

Peninsula (Sutton & White 1968; Stewart,

‘Slade & Sutton 1973) and possibly this reflects

the relative instability of the margins of the

Peninsula compared to its interior. ‘Thus late

Cainozoic faulting has heen Gemonstrated

(Miles 1952) over a wide area be(ween

Whyalla and Cowell and suggested for the

north-western margin) in the eastern purt of

the Nullarbor Plain (Jones 1880; Jennings

1963).

These ureas. are however remote from the

feature under discussion where, within and

at the margins of the Corrobinnic Depression,

there is no evidence of any recent dislocation

of at order adequate to explain the topo-

graphic low. This conclusion is necessarily

tentative for small fault scarps may have

developed only to be obscured by alluvium ar

sant drifts, But on the available evidence the

Depression originated by faulting in the dis-

tunt past, There is no evidence of recent 1ec-

tonism of geomorphological significance in the

vicinity of the Depression. It seems more likely

to be # fault zone of great antiquity which has

heen subject to recurrent jogeling.

The presumed fracture zone separates dis-

unct lithological provinces, for apart from

some (?)Archaean sediments in the Mt

Allalone area and granitic outcrops at and

around Numimee and Waulkinna hills and in

the Bucklehoo area (Fig. 1), the area north

of the Depression is occupied by the Gawler

Range Volcanics (Fig. 3), a predominantly

dacitic lava flow but with some rhyodacites.

ee ee eee

1Bovd, D. (1970), —Eyre Peninsula: Regional Magnetic Interpretation (121,000,000). Unpublished

map, Dept. of Economic Geology, University of Adelaide.

142 JENNIFER A. BOURNE, C. R. TWIDALE AND DIANNE M. SMITH

ELLISION 7TAQUGH

AUSTRALIAN

BIGHT

oe rata

road

trirk,

. aNtelinal se S

oy Uptends

eye WHI

pia —" —

BE . h,

(AEF a \I

ZSARaner

coh ois

bitty wos

Fig. 3, Regional location map and major geological! structures of northern Eyre Peninsula. Compiled

ftom existing geology maps and field data.

and rhyolites (A. H. Blissett, pers. comm.) of

Precambrian age and dated by radiometric

means as being of the order of 1,535 million

years old (Compston, Crawford & Bofinger

1966; Compston & Arriens 1968). To the

south and south-west of the Depression, on

the other hand, the bedrock is essentially

granitic, Admittedly at Mount Cooper and on

Hurt Island (in the Nuyts Group, some 80 km

SW of Ceduna) there are small outcrops of

porphyritic rock but they are of very limited

extent und are in any case not of Gawler

Range type. Also, though certain discrepancies

have appeared in the dating of granitic and

gneissic basement rocks of Eyre Peninsula,

their reported ages are in the range of 1,590—

2,800 nvy. (Thomson 1969, pp. 30-31). Thus

whatever the details of the relative ages of the

various masses of granite and gneiss, they are

consistently older than the Yolcanics.

The limits of the suggested fault zone are

reasonably clear in the south-east where it

extends at least as far as Spencer Gulf; in the

Cleve Hills there are exposures of deformed

Precambrian sediments and metasediments the

folds of which are truncated by a linear siruc-

tire running NW-SE through Cleve (Fig. 3),

To the north-west however, the fault zone

gradually fades. There is neither morphalogi-

cal nor geological evidence of its continuation

beyond the Hundred of Toondulya. Furiher-

more the stratum contours of the base of the

Tertiary rocks in the Eucla Basin (Tectonic

Map of Australia 1960)? give no indication of

* Published by the Bureau of Mineral Resources, Geology and Geophysics, Department of National

Development, Canberra.

THE DORROKINNIE DEPRESSION 145

tongiing soulh-easiwards toward the Depres-

sion,

Streuerire of the Depression. Whether the

Corobinnie Depression is essentially a tectonic

oro structural feature cannot be determined

with any certainty. tt could be seen as occupy.

inga graben which has largely been filled in hy

detritus Washed in from. the adjacent areas.

The feature is long gnd narrow and though

there is some offsetting of the margins all

these features are characteristic of known

graben, The prominent Sranile ndge running

through the Minnipa and Wadinoa districts,

south-west of ihe Depression, could be an adja-

cent horst or anticlinal block (Twidale 1964),

Corrobinnie Hill anc Peetla Rock could be

regarded as minor horsts or ws components of

# single borst hlock within the major depressed

structure. Paraholic dunes are closely associa-

ted with the Depression and their distribution

south-east of Kina suggests that one branch

al ihe postulated fracture zone bifurcutes in

i# manner iypical of known graben (Twidale

1971, p, 121). However none of this evidence

is conclumve and can he interpreted in other

Ways.

The Depression could occupy u fault-angle

valley similar to that which occurs to thr

south-west of the feature under discussion, in

the Polda Basin (Rowan 1968) and in its

westerly submarine extension in the Elliston

Trough «Smith & Kamerling 1969), Only one

fault has been identified by geophysical means

und the two structures together are regarded

xs a Eaullangle trough in which are preserved

Mesozoic and ‘Tertiaty strata {Harris 1964:

Rowan 1968; Smith & Kamerfing 1969}.

Support for the view that the Depression

occupies the site of an ancient fault-anele

structure derives from the gross morphology

of the Gawler Ranges which are delimited on

their southern margin by a series of faults,

The uplands rise abniptly from the plains to

the south but slope gently down to the north.

They could be viewed in gross as a fault-tilted

block, with a prominent though naw much

dlissecied Fault scarp forming the southern

boundary of the Ranyes and the northern limit

of the Corrobinnie Depression. If this inter-

pretation is correct. the faulting responsible for

the tilting was active during the early Creta-

ceous for high energy streams from the (re-

cently uMifted?) Ranges carried pebhles and

houlders of Gawler Range Yolcanics to the

north where they occur jy strata of early

Cretaceous age (Wopfner 1969, p. 152).

However this is speculation. There is no

uneguivocal cvidence that the Corrobinale De-

pression is tectonic. If it Were initiated as a

graben or tault-angle depression then the tec-

tonic outlines of the feature have long since

heen blurred and obscured by Weathering,

erosian and deposition.

An alternative possibility is that the Corro-

binnie Depression is not primarily tectonic but

is of structural origin sense sireio\ ie, it has

tvalved through the exploitation of a major

fracture zone by agtats of weathering and/or

érosion. If this were so then Iwo miujor ques-

tions arise:

What agents aze Yresponsible for the

development of the Depression? This prob-

lem in turn necessitates a consideration of

the age of the feature,

2. Why has the fracture zone to which the

Corrobinnie Depression owes its otigin

been exploited ro a much greater extent

than the others which evidently are present

in the region?

Formation und age of the feature. Though the

faulting to which the Cormbinnic Depression

is related is probably of great antiquity, this

provides no real measute of the age of the

feature under investigation. The only evidence

relevant to this question cetives From a bore

located some 12-13 km west of Balumbgh

und logged by R,. G. Shepherd (S.A. Geol.

Survey, Report Buok 67/113, Bore 6-0),

Hundred of Panitya). This bore is Jocated at

the margin of the Corrobinnie Depression, bot

it is typical of the Depression us indicated by

a comparison with Bore 20-1 (Hundred of

Carqlye) lovated some 2 km to the SSW. The

latter ran through less than 6 m of sand hefore

penetrating the gneiss basement, whereas 6-01

penetrated some 50 m of sediment before

reaching the weathered granitic bedrock. The

upper two thirds of the sedimentury fill con-

sisted of sand, gravel and clay assigned to the

Pleistocene arid Recent, but within the lower

third, which also consisted of gravel. saud and

silt, was a lignitic horizon which ts compared

with known Lower Tertiary lignites at Kopi

(Fig. 1) and other shallow basins on Eyre

Peninsula, It is cmphasized that this is extra-

polation and is not based on un examinution

of the contained organic materials, of which,

unfortunately, none were preserved (W. K.

Hareis, pers, comm.). Bat if this interpretation

ig correct, then clearly the Corrobinnie Depres-

sion was already in existence as 4 topographic

feature by the Eocene,

\44

If the Depression were essentially inizisted

during the laler Mesozoic of the earliest Ter-

tiary, then it is im relation la the climates and

conditions of these times that its mode of for-

mation should be sought, Apart from

dreikunter found in the present Lake Eyre

region in strata of Upper Jurassic age

(Wopfner 1969, p. 147). there is no evidence

and no argument from general considerations

(Brown, Campbell & Crock 1968, p. 245 ef

seq.; Wellman, McElhinny & McDougall 196%,

Embleton 1973) pointing to deserlic condi-

tions in or in the vicinity of northern Eyre

Peninstila at any tine from the later Mesuzoic

until the Tale Pleistacene, ‘Vhough aeolian

action is responsible for moulding much of the

present surfice of the Depression, it is difficult

lu substantiate aby argument which attributes

the erosion of the feature to wind action,

Two agents of degradation that warrant

serious consideration are rivers and weather-

ing.

It nwy be argued that the fracture zone

has heen preferentially weathered because the

faults allowed ready penetration nf ground-

Water Which aliered the cock with which it

cate into contact within and adjacent ta the

fracture zane, This weathering niwy have con-

Iributed to che formation of a tepographic

depression either by permitting ready stecam

erasion, ol by causing volume reduction of

the bedrack and consequent lowering of the

land surface.

If sireums hud Nowed in ated caused the

lowering of the floor of the Depression. there

should in theary he seme evidence of an outlet

through which water and sediment were evacu-

ated. No such outlets have heen located

though litte inforihation is available concern-

ing the morphology of the hedrock <turfoce

beneath the cover af surficial materials. At its

south-castem extremity the Depression ter-

minutes ugainst Wie recently upfaulted Cleve

Hills. and there is very litle data concerning

ihe stratigraphy of the sediments deposited

in the relevjint pant of Spencer Gault. To the

north-west and west there is no evidence to

band of a former outlet ether lo the Great

Austealian Bight or to the Eucla Basin. IF the

Corrobinnig¢ Depression were in existence as

long ago as the early Tertiary it is perhaps

Wnreascmuhle 1a expect to find evidence of

ancien) stream courses still preserved at Unis

tine. ‘hus it cannot now be proved that the

Corrobinnie Depression is 1 faldine vulley-

JENNIFER A, BOLRNE, C R, TWIDALE AND DIANNE MM SMICH

An alternative mechanism which should be

vonsidered is based on value decrease of

granitic rocks consequent WW pon intense chemi-

cal alteration, which cun be inferred to bring

ulout iu significant, even a dramatic, reduction

in volume. Ruxton {1958} has suggested that

as much as 50% by volume of granite hed-

rock inuy bg lost either in solution or as fines

as a result of intense weathering and suhsur-

face flushing by water. Outcrops of intensely

weathered granitic gneisses have heen reported

from tow shoreline cliffs of salinas within the

Depression {Shepherd 1961) and ihe stepped

morpholopy af Corrobinnie Hill argues.

repeated weathering and lowering of the

granite hedrock to a total depth of at [cast

15 1m. Thus rack types prone ta yolume reduc-

lion of chemical attack occur within the

Depression and there ts evidence that they

have been subjected to such alteration,

There can be little doubt that where there

is A repeated accession of water to attack and

flush the bedrock, as fer instance in the scarp

foot zone of granitic residuals In West Atricn

{Clayton 1956), the Libyan Desert (Duman-

owski 1960) and Eyre Peninsatla (Twidale

1962, 1967), this process of alteration, Nush-

ing, volume decrease and surfiuce subsidenee

could be an important contributory factor in

the development of scarp font slepresstons

(Fig. 9). But these are minor forms; whether

such o process could account for uw regional

festure like the Corrobinnic Depression is

questionahle. The evacuation of fines and

solutes from the Depression would require an

hydrivlic vradient away rom the posiulated

fault Zone, a condition which could only be

achieved by assuming that the cewion Ja¥ well

ahove sea-level throughout the period of

development and that no geological burriers

intervened fo prevent the escape of the sub-

surface waters,

Morcover there ts no peneral agreement

that chemical wleration of granite everywhere

results in volume decrease and surface sub-

sidence, Thanras (1966) has pointed out that

in Nigeria deep weathering of granitic hed-

tock is not reflected in the development of

lopographic basins, Ollier (1969, p ISP) has

challenged the general concept of surface

Jowering consequent on weathering presented

in relation to the formation of taterite in East

Africa (Trendall 1962), poiniing to evidence

of alteration which has taken place with no

significant veliime change. Qn the ether hand,

ihe volume increase consequent on the

THR CORKOBINNIE DEPRESSION

weathering of certain clays is commonly culled

upon in explanation of certain Features ane

forms, such as gilgai.

These severs| difficulties are not denied, Ih

may he that the character ot the volume

chinge, if any. fesulting frum chemical

Weathering varies according to climate and

vegetation. and benee the chemicul nature of

the groundwaters, and upon whether the sts-

fem is open of closed, Certainly the course of

chemleul weathering and the end products of

such changes varied with these factors (Lough-

nan L964, p. 27) ond it may he that volumet-

nice changes vary also,

In light of these problems und uncertaintics

it is possible only ta indicate what may have

occurred rather than what did take place, The

Carrolinnie Depression could have originated

in seyeral Ways. It could have a composite

rigin, Et could for instance have been initiated

a5 a Ewull-augle depression durin the Jater

Mesozwoi¢, heen further exploited by a tiver

system or systems the outlel of which is no

longer in evidence, and been further enlarged

as a result of volume decrease consequent upon

ihe intense Weathering of the granite and gneiss

basement. Alterhatlyely, any tectonic disloca-

lions which occurred during the fater Caine

zo aod which are invoked to achieve the

elusure of the Depression and the truncation

of any pre-existing externa) drainage, may

fave tniliated the partial infilling of the De-

pression which ts evidenced by the cover of

Plelsiocene sand, gravel and silt.

Distinetive development of the Corrokinnie

Depression, The Correbinnie Depression js

unique due to the juxtapesitian of the Corro-

hinnie Fault Zone and the resistant and up-

standiig Oulermp of the Gawler Range Vol-

canics. Other fractures suggested by geo-

physical survey and geomorphological expres-

sion are developed larecly in granitic tucks

and haye pot achieved such marked topo-

gtaphic expression, There is little relief adja-

cent to them, and in consequence little runoff

ro the fracture zones and therefore no great

Hispitity OF Weathering between the fracture

Zone und the surrounding country rack.

North of the Corrabinnie Fault Zone on the

other hand, the hills of the Gawler Ranges

s(and Up to 300 m above the valley floars and

a large part of the upland region trains to the

lowland which borders it on its southern side,

Me. Jatin Kwaterski, Senior, al) aatly ugricul-

turilise Of the Miniipa district and explorer of

14)

the Depression, reports (hat alter heavy rains

in the Gawler Ranges arcat shallow sheets of

water stand for a few days m the Depression,

Thus in T8946, Which was a year of above

mvernge rainfall throughout norlherm Eyre

Peninsula (Mtnnipa recorded 48 em compared

with jin annual average of 35.1 cm, and

Yardea 40.3 cm against the usual 27 ent). the

salimas in the Depression carried over 2 m of

water. He has also heen told that in 1890 the

Minnipa—Yardea road was covercd by water

where it passes through the Depression: though

this information is second-hanid its accuracy

is borne ouc by the fact that the rainfall

records show that year also tq have been

one Of unusually heayy rams in the district,

with Yardeu for example receiving 43.3 em.

Quite apar. fram present lendencies, there

is evidence of an cven greater former influx of

water to the Depression from the Gawler

Ranges. Relicis of a now disrupted and dis-

membered formet' druinaze system in the form

of -strings of salinas and curvilinear depres-

sions, which link them and which contain

weathered alluvium, attest to the presence in

former times of a well-developed drainage

system Mowing from the present Thurlga and

Mi. Ive properties to the Corrolirmie Depres-

sion. The width of the meander belt delineated

by these relict forms is approximately 1) km

(though it cannot be measured with ceriamly

heeause of subsequent mudificalion of the

castern shores of the Inke by Iunemes}, cons-

pared with 1.5 km for the present stream

courses. This. surely suyeests a drainage sys-

jem of much greeter discharge than the

present streams achieve cven in times of flocd.

Thus although there are simitar fracture

vones elsewhere on the Peninsula and in the

arca to the north, only in the vicinitv of the

Corrohinnie Depression are there rocks other

than granite. Thus it is only there that there

ure uplands of any consequcnce and hence

only in this area is there a disproportionately

lurge runoff ta ane of the fracture zones. This

is the reasom for the Corrobinnie Fault Zone

alone having developed into « feature of

regional topographic significance, Topographic

lows, such ax that occupied by Lukes Yaninee,

Wannamans and Warramboo and Kappakoola

Swamp (Fig, 3}, appear to be coincident with

another possible fracture zone hut it is neither

as well nor as extensively developed, pre-

sumably because of the presence of granite

bedrock throughout the area and the absence

of any upiand areas of significant extent.

le IENNIFRR A, BOURNE, C, R, TWIDALE AND DIANNE M. SMITH

These then are the reasons for the evolufion

uf the Corrobinnic Depression and lor its heing

a mujor constituent of the geomorphological

frankework of Eyre Peninsula,

Landforms

The Jandform ossemblage within the Corro-

binnie Depression differs greajly from those in

adjacent areds and comprises principally

silinas and dune fields, The granite hills which

ate present are broadly similur to those <es-

cribed from other parts of north-western Eyre

Peninsula (Twidale 1962, 1971, pp. 4-96),

though one, Corrobinnic Hill, is sufficiently

distinctive to warrant description and explana-

tion, In addition there are within the Depres-

sion a number of characteristically rounded

pacphyry hills, The highest is the upland com-

plex of Mt. Sturt which nses abmaptly from the

lowlands,

The salinas, These occur in a few extensive

zones within the Depression, and especially

toward the seriliwestern extremity (Fig. 1).

Many carry a halite crust though the edges are

commonly sandy or muddy, Some of the

smaller salinas nestle amongst the dune ridges,

hot the tatger ones are bordered by chits up

to 7 m high in which are exposed dolomitic

silts anu silicified dolomite, Similar outcrops

oceur in the cliffed margins of islands within

the Iskes, and, like the bordering cliffs, are a

measure of the Inwering of the lake beds in

recent times. The dolomilic sediments are af

lncustrine origin and represent 4 higher level of

lake accumulation. Unfortunately the sedi

ments appear unfossiliferous sa that it is not

possible at present to date the erosion (de-

tiation?) responsible for the lowering of the

greater purts of the playa depressions anc the

development of islands ani! cliffs.

The dune felds. The greater part of the Corra-

binnie Depression is occiipied by Quuternary

sands. There as onty one bere which penetrates

through the sands to the undertying bedrock.

and as mentioned previously this passed

through some 50 m of sand before reaching

weuthered bedrock. Elsewhere the thickness

of the sand has to be inferred. For instance.

weathered gneisses are exposed in und around

salinas south of Mt. Sturt so that the eleva-

tiun af the dunes above these salinas provicles

a measure of the thickness of the sands, and

on this basis the Jatter seem to be 30-40) m

thick,

The sund conld have been blown into the

Depression by the wind from adjacent areas,

it could have been washed In or it might have

formed essentilly m1 site due to the weather-

ing of the underlying granitic bedrock within

vod adjacent to the fracture zone; or it could

hove been derived from all three sources,

The sands are overwhelmingly ub quartz

though there is about 79% by weight of fines.

The sands ate pfedominantly in the fine—

medium tange (Fig. 4), being mainly m the

range 0.105--0.335 mm, Some of the grains are

quite well-rounded but most are angular to

subanuulur, The rounded grains display frost

ing and reddish brown haematite staining is

eummon. The clay fraction of the fines acts as

f cement, lor the quarry fragments are com-

monly in the form of aggregates of unwashed

sand.

The anguluc character of the balk of the

sands. suggests thit the sands are locally

ilerived; they have probably been washed or

blown into the Depression from the

immediaiely adjacent areas. The larger,

rounded gryins probably represent sand which

has been transported along the axis of the

Depression either by wind or by ancient rivers.

Ferruginised and mottled sands are exposed

in the Depression nurth of Wudinna, The

lerruginous indurattons have presumably

formed at the base of dunes and close to the

water table and are dye tu the iluviation of

iron salts and their precipitation at lower

levels; similar accumulations have been noted

low on the flanks of late Pleistocene dunes at

Agars Lake, near Minnipa, north-western

Eyre Peninsula. Culcrete is also well developed

in the dunes. Assuming that this pedogenic

accumulation began soon after relative stabil-

isution of the sands, it provides a means of

dating the deposits. Samples of calerete close

to Corrobinnice Hill and trom dunes neur the

southern marvin of the Depression 25 km

ENE of Wuilinna gave dates of 15,780 + 350

(Gak 3451) und 22.040 = 760 (GaK 3452)

respectively, indicating that the sands are at

icasl of late Pleistocene age.

The surface of the sand has been moulded

by the wind and shaped into dunes mainly ol

parabolic type, Dunes which are reticulate or

box-like in plin also occur it some areas.

There are also patterns which while broadly

rectangular ar rhomboidal in plan are less

angelar than the truly reticulate forms As

these are thought possibly to result from the

ileflation of sand from the hollows and leav-

ing the ridges ay residual forms, they are

termed alveolar CeP. Féderovitch 1944), Also

THE CORROBINNIE DEPRESSION

100

50+

w 30

2 20

Eq 10

mo]

9 at

Q se me nm

Phi() se 8 2 a é

= oO

mm : : - .

wen gs 8 os Be eR

147

he w we » oa

th a thy 3 Mn

A : , - 2

NS Ff Bp BS Oo o-oo oOo Oo 46

=_- N FR HBS GQ

oN 0 &© GD BYP & B&B € EZ

Fig. 4. Graphs showing grain-size analysis of sand samples, the locations of which are shown on Fig. 1,

present are true dunes which are almost circu-

lar and form either in the lee or to windward

of obstacles (Fig. 7). It is not uncommon for

several ridges to be arranged concentrically in

such circular patterns.

The deep sands and vegetated surface

favour the development of parabolic types, but

the concentric dunes and particularly the long

diagonal straight ridges of sand (Fig. 5) are

unusual, It seems that the ridges formed in

response to a W-NW wind as ordinary linear

sand ridges or longitudinal dunes aligned

parallel to the vector of the varied but esscn-

tially NW-W winds (cf. Simpson Desert—

Wopfner & Twidale 1967; Twidale 1972); they

were then stabilised by vegetation. The wind,

possibly from a slightly different direction

(either present day secondary winds or former

ones of a different wind regime) may then

have blown out some of the linear ridges into

parabolic dunes.

The wind shaping the linear dunes was W-

NW, as attested by the encroachment of some

of the ridges on to the western margins of

14% JENNIFER A. BOURNE, C. R. TWIDAILE AND DIANNE M. SMITH

Tiz.

5. South-castern extremity of Corrobianie Depression showing majur purabolic dunes, linear con-

necting sand ridges, and Jongitudinal dunes to NE and SW. (Drawn from air photographs. )

sitlinas, und by the downwind convergence of

ridges. However u consideration of the Kyan-

cutta wind rose shows that at present the

sand-moving (i.e. 11 knots (20.4 km/hr) and

over) winds are from the south-western sec-

tor. This implies that the dunes of the Depres-

sion. which are here called the Kwaterski

Dune Field after the pioneer and friend to

whom earlier reference has been made, were

formed under a very different wind regime,

imd ure thus suggestive of climatic chunge.

Evidence of a similar late Pleistocene change

in climate and wind regime has been adduced

in the Riverina districts of western N.S.W.

and northern Victoria (Bowler er al. 1970,

Bowler 1971). However there is no evidence

from the arca under discussion of an age

contrast between the parabolic dunes of the

Corrobinnie Depression and the longitudinal

dunes of the area to the south. As mentioned

previously calercte from the sands of the

Kwaterski Dune Field gave dates of ulmost

16,000 and just over 22,000 years B.P. (Gak

4351 and 4352), Similar material from the

linear dune field provided dates of just over

10,300, almost 16,700, and almost 27,000

yeors B.P. (GaK 4071, 4072, and 4639).

Thus the sand within the Depression is of the

same order of age, and falls within ihe same

range as Lhat of the longitudinal dunes.

The granite forms. Two granite hills stand

above the level of the duce complex. Peella

Rock is a low whaleback which displays flared

slopes, gnammas, many of them developed

along joints, and boulders with tafoni; ie,

many of the minor granite landforms com-

monly evolved and exhibited on granite

residuals of southern Australia (Twidale 1971,

pp. 80-96). Like many other granite outcrops

of northern Eyre Peninsula, Peella Rock has

in the past been used for water conservation

and an claborate scheme of gutters and drains

leads runoff from the bare rock surface to

storage tanks (Twidale & Smith 1971).

Corrobinnie Hill is both more extensive and

stands much higher ihan does Peella Rock

which is located some 2 km to the south-west

(Fig, 1), The inselberg displays multiple flared

slopes, sheet structure, magnificent tafoni,

gtlammas, wedges and boulders superimposed

on a curious cottage-loaf shape, with one large

THE CORROBINNIE DEPRESSION

= a a Wh imal

Sak

KOK ,

1 \ *

! “eT I

i\|

' / i \ ‘ i

NUE HIN ME AL

u ee

Gonlour interval, oS neves

OU inesse 500

ekoused rack

Fis. 6, Corrobinnie Hill showing the inselberg

and the areas of granite ovtétop sur-

rounded by sand plains and dune fields,

boulder or turret rising above a broader mass

oF rock, and with this in turn resting upon an

extensive platform of granite (Figs, 6 and 10).

Corrobinnie Hill (Big. 6) rises via a narrow

step to a broad even surface which stands

some 15 m above this broad granite platform,

the level of which is coincident with that of

the surrounding sand surface. This suggests

that the granite mass may have suffered re-

peated weathering and planation by moisture

(Twidale 1962; Mabbutt 1966) held within

the sands Japping up against the flanks of the

hills: The moisture could disintegrate the rock

and cquse the granite slope both to he

149

stecpened and to recede, forming the platform

which presently surrounds the residual. If this

were the case a recession of the order of S00-

706 m is indicated by the platforms nearby and

extending to Corrohinnie Hill, Presumably far

more ime than the twenty-odd millennia indi-

cated by the Cl4 date cited above for the age

of the dunes ts implied, This last date probably

indicates the time of the last onset of’ aridity

and calcrete accumulation whereas sands had

heen in the Depression at much the same level

for some time previously in order for the

planation of the inselberg to have occurred.

Thus a measure of equilibrium in the Depres-

sion between the accession and evacuation of

debris is inferred,

Subsurface weathering, which is the essential

pteparation for the extensive planation, must

have occurred when the sand surface stood

perbaps 5-6 m higher than at present: lured

slopes of this order now border the main mass

of Carrobinnic Hill and suggest a land surface

Which stood level with the then upper extremity

for some considerable time, Since that rime

the sand and weathered granite have heen

eroded from the higher areas near the uplanu,

exposing both the flared slopes: and the esscn-

tially plunute Weathering front in granite as an

etch surface. The calerete uccumulated in the

sand cover on the gronite platform and is pre-

served on lower slopes, Thus the late Pleisto-

eene date for the calerete near Corrobinnie

Hill provides a2 minimum date for the granite

platform.

Conchision

The Corrobinnie Depression is characterised

by an assemblage of landforms which differs

greatly from those on either side, The Depres-

sion is considered to be basically a weathering

feature. It is due to the exploitation of a major

fracture zone in the granitic bedrock of

northern Fyre Peninsula by waters flowing

from the southern Gawler Ranges.

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Compson, W., Crawrorp, A, R., & BOrFiNueR.

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Comeston, W. & Arrmns. BP. A. [1968).—The

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(ANU. Press Cankerra.)

Fie, 7. Part of the Kwaterski Dune Field showing parabolic and igfegular dune forts, in particular

the ciredlar dune complexes (A) conmiprising patterns of concentric dines. Longitudinal dunes

are seer in bottom lett of photograph. (Reproduced by permission, S.A. Lands Depurténentt.)

Fig. 8. View across Corrohinnie Depression from Chilpnddie Hill (Fig. 1), showing granite houlder

und pavement in foreground, salinas im far middle distaiice and Gawler Ranges in backgrownd,

(Cc. R, Twidale.>

Pio. 9, Shallow depressions or moata at base of granite residual north of Wudirma. ¢C. R- Twitale.)

Fig. 10. Coerobinnie Hill stands sume 15 m above a pitted grunite plarform (foreeround) pmd is sur-

mounted bY a prominent tower, also of granite, (C, R, Twidole)

THF CORROBINNIE DEPRESSION

JENNIFER A. BOURNE, C. R. TWIDALE AND DIANNE M. SMITH

sitesi

STRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA

BY J. B. FIRMAN*

Summary

FIRMAN, J. B. (1974) .-Structural Lineaments in South Australia. Trans. R. Soc. S. Aust. 98(3),

153-171, 31 August, 1974.

Particular linear features can be seen on photo-mosaics at a scale of about 1:63.360. Some sets are

better developed in one natural morpholithological subdivision than another. Sets trending

approximately NW, NNW, NNE and NE are more common than sets trending WNW and ENE.

The features have been compared with geological and geophysical patterns and trends. There is

reasonable agreement between patterns and trends of the linear features and of geological features

on maps at scales as small as about 1: 1,000,000, and quite good agreement between linear features

and geological and geophysical features at scales of 1:250,000 and 1:63,360.

The comparison of maps of linear features with geological and geophysical maps shows sufficient

correspondence of patterns and trends to confirm that particular linear features on photographs are

structural features. The persistence of these features as straight lines through different landscapes

suggests that they are planar structures with a vertical dip. For these reasons the features have been

named structural lineaments. Their development appears to be associated with major tectonic

events such as warping of the basins and uplifting of the ranges, and it is suggested that they reflect

profound structures and tectonic elements in the crystalline basement.

Structural lineaments appear to post-date very young deposits, and to be cross-cutting with respect

to Palaeozoic and older fold trends. They also outline basin margins and the structural boundaries of

crystalline basement and, in these situations, may be rejuvenated structures as old as the time of

formation of the basins and the time of origin of the welded blocks themselves.

Because the youngest structural lineaments are parallel to old structural features marking the

margins of ancient blocks, it appears that there has been no major disorientation within the study

area of even the oldest structural units.

STRUCTURAL LINEAMENTS IN SOU'LIL AUSTRALIA

by J. B. Firnman*

Summary

Pmean, J. B, (1974)—Structural Lineaments in South Australia. Trans. &. Soc. S. Atest, 98

(3), 153-171, 31 August, 1974,

Particular linear features can be seen on photo-mosaics at a scale of about 1:63,240.

Some sets are better developed in one natural morpholithological subdivision than unother.

Sets trending approximately NW, NNW, NNE and NE are more common than sets trending

WNW and ENE.

The features have been compared with geological and geophysical patterns and trends.

There is reasonable agreement between patterns and trends of the linear features and of

geological features on maps at scales as small as about 1;1,000,000, and quite good agreement

between linear features and geofogical and geophysical features at scales of 1:250,000 and

1;63,360.

The comparison of maps of linear features with geological and geophysical maps shows

sufficient correspondence of patterns. and irends to confirm that particular linear features on

Photographs are structural features. The persistence of ihese features as straight lines through

different landscapes suggests that ihey are planar structures with » vertical dip, For these

feasons the features have been. named s¢rijetural lineaments. Their development appears to be

associated with major tectonic events such as warping of the basins and uplifting of the

ranges, and it is suggested that they reflecl profound structures and tectonic elements in the

crystalline basement.

Structural lineaments appear to post-date very young deposits, and to be cross-cutting

with respect to Palaeozoic and older fold trends. They also outline basin margins and the

structural boundaries of crystalline basement and, in these situations, may be rejuvenated

structures as old as the time of farmution of the basins and the time of origin of the welded

blocks themselves,

Because the youngest structural lineaments are parallel to old structural features marking

the margins of ancient blocks, it appears that there has been no major disorientation within

the study area of even the oldest structural units.

Introduction

Extensive patierns of rectilinear fractures—

including joints and major faults—were first

Observed by the author during field-work for

the Bureau of Mineral Resources in the Dar-

win-Katherine, Georgetown-Einasleigh, Calvert

Hills-Robinson River, and Port Headland-

Ripon Hills areas in Northern Australia during

the 1950's. The regional extent of these lineat

features became apparent when the author

compiled early versions of portions of the

1960 Tectonic Map of Australia, including

Western Australia, the Northern Territory arid

parts o£ Northern Queensland. Later phato-

interpretation of areas in the Northern. Terri-

tory between the MacDonnell Ranges and the

Victoria River Basin revealed similar recti-

linear patterns, in this case in sparsely vege-

tated and soil covered aveus.

The recognition of similar features in soil

covered areas in the Murray Basin of South

Australia from low-flying aircraft and on

photo mosaics led to a study of these features

in 1966 (Firman 1970). The work was con-

tinued in later years when student geologists

from the University of Adelaide and other

geologists from the Geolovical Survey of South

Australia assisted the author to identify and

plot the lineaments on available 1;63,360

photo-mosaics for the rest of the State. In

1972, 4 different method was used to compile

a map of lineaments in the Great Artesian

Basin on the easiern margin of the State, In

1973, compilation was contiaued using other

motheds for lineaments in an area including

* Geolosical Survey, S.A. Department of Mines, Adelaide. S. Aust. 5000,

154

the eastern Eucla Basin and the western mar-

gin of the Gawler Block (see Fig. 1).

The paper begins with a brief description

of the lineaments, discusses different methods

used to compile maps of the lineaments, and

concludes with a comparison of the lineaments

with geological and geophysical features.

Structural Lineaments

For reasons set down in Firman (1970) and

fuborated later in this paper, the particular

MAJOR TECTONIC UNITS OF

CAMBRIAN AND PRECAMBRIAN AGE

MAO) EROLOIG

SUSTALLINE BASE HENT PROTEAN ZO COVER ROCKS

3B Seuare Sael= ayer

Mulgrave Block S OVoriam Bayemny ae

Gakwler Blozk> Gawler

Range Vetere; and

akpored-larian Bayemene _ Bodhiat Geelaneiiag

CARSRIAN

Keywiantsu Trougy ane

Hipa

WHipid BIBL Delameran Bsjenieni

Precambrian crystalline bosemenr uideriees oes, =

LS a a

KILDMETNES {00

WOOT RO ihe re tebe

42-2 Del) Loe

TRE ITOR®

J. B, FIRMAN

features appearing on photo-mosaics and

described in lhe introduction as "linear

features” have been culled “structural Jinea-

ments”. ‘The Jinear features appear as local

features on individual mosaics, but these can

be traced through other mosaics for great dis-

tances, or can be seen to be parallel to other

similar features having regional extent. There

can be, therefore, no simple classificatian into

separate “Jinears” of local extent and “linea-

ments” of regional extent as defined by Dennis

= 7

_ SLU ERSSL AND

ho es py

ee ed

—.

Chie Hhavelerateenie

brash

J KILOMETRES

12 Farming 11972)

Fig. Lt. Locality Map, Morpholithological subdivisions in South Australia.

STRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA [ss

(1967), Although same local features are

obviottsly joints, there are also local features

known to be faults, sa there ts no simple

classification possible into local “lincars”™ which

are joints and regional “linewments” which are

faults. Huntington (1973)? uses “fracture

trace” to describe the kind of feature described

herein. Unfortunately, some of the topographic

and other features included in his definition

have been specifically excluded from the defini-

Gon Of structural lineaments because they are

wat the particular features recognised on photo-

mosuics in this study. For these reasons, the

names “linear” and “fracture trace’ have not

been used,

“Structural lineament” jas used herein refers

to straight linéar features, The features mark

structures which are mainly, but not exclu-

sively, fractures (faults and joints). They have

both local and regional expression. The struc-

tural lineaments described hercin occur as par-

ticular features on photo-mosiics, al a scale of

about 1:63,360. On photo-mosaics of larger

scale and smaller area—or on individual air

photos—the hneuments cunnot be seen so

easily. There is no doubt thut structural linea-

ments also have expression on other imagery.

Lineaments are real for the following

reasons: They cun be seen in the zone of

overlap of individual air photos taken at dif-

ferent times from different places, and they are

also traceable across adjoining runs in each

1:63.360 photo-moszic (where at least four

different air photos gre involved) and from one

phote-musiic to pnother, Lincaments can be

seen from low-flying aircraft, and they have

been. checked in this way between Adelaide

and Coober Pedy, Adelaide und Port Augusta

aand Adelaide and Renmark.

There appears to be no unique reason con-

nected with rock type or topography to explain

why lineaments should be so clearly visible,

The. lineaments are equally well defined in ter-

rain developed on crystalline basement—Wwhere

they are parallel to jointing in outcropping

rock—and on terrain developed on fiat-lying

sediments. In folded sedimentary sequences,

most of the third order landforms reflecting

fold structures appear to have no relationship

at ull to the lineaments which cut across them.

In faulted arcas, some lineaments lie along or

closely parallel to fault-line scarps where struc-

tural control of landform is clear. Other linea-

ments in these areas appear to have na rela-

tionship to third order landform wt all. It is

suggested that the lineaments are the result of

jointing and faulting, and that they can be

seen and photographed even in soil-covered

areas Of no obvious topographic conitrust

because vegetulion changes occur along them,

probably duc to moisture variation within the

zone penctrated by the roots of growing plants,

A ground check of structural lineaments has

been made at various places in the Murray

Basin fsee Figs. 9 and 10 for locations).

Examination of terrain along the Morgan

Fault, Marmon Jabuk Fault and Kanawinka

Fault {Lincament), which are all marked by

‘Huntington, J. F. (1973).—Fracture Anulysis. Jn “Photo-Interpretution for exploration and survey

geologists". Australian Mineral Foundation [Tnc.). Study Course (unpubl.).

MORPHO-LITHOLOGICAL SUBDIVISIONS

Wealero Aanins

1 ODPFICER BASIN

PROVINCE

Western Shield

2 GAIRDNER PRO.

VINCE

Coke Galrdner aves

Central Busius

It] TORRENS BASIN

¥ROVINCE

Hightand Chain Eastern Basins

|, MUSGRAVE It GREAT ARTESTAN

RANGES PROVINCE BASIN PROVINCE

Peake ancl GBenisen

Ranges

3, CENTRAL

KANGES PROVINCE

Minders Ranees

OMlary “Ranaes'”

Vv_“FROME EMBAY-

MENT PROVINCE

Yl SPENCER RASIN

PROVINCE

VY EUCLA RASIN

PROVINCE

Eyre Peninsula

VII ST: VINCENT Mr.

VU MURRAY BASIN

Lofty Kanges PROVINCE

BASIN PROVINCE

Kanenron Istand

6. to 1X Padthoway

Ride

IX OTWAY BASIN

PROVINCE

INFRADASINS

A Pédirks Usdin RB Arckazinga Basin

D Boorthenny Trough E Copper Basin

Tiouely

154

stinictural Ilfeaments, shows the ustul features

stiguesting fuulling. These include fault-line

scarps and linear third arder landforms parallel

to (he structure (and the structural linea-

micnts), ahd juxtaposition of different naterials

st the surface or tn bores. Sprigg (1952, pp.

32-38) records delaniitization of small faults

and jaints marked by secondary catcium car-

bonate which appear to mutch regional struc-

turul trends im the south-east of South Aus-

tralia. No separate unique feature appears to

mirk ihe lineaments. Elsewhere, for example

at some places in the Murray River cliffs, weak

fracturing is the only structure matching struc-

tural lineaments, Neither lineuments markine

the Encounter Fault Zone nor those marking

the Hamley Fault have surface expression in

busin sediments. although a tmonocline aficct-

ing the Morgan Limestone is exposed in river

cliffs neat where the matching structural ligea-

ment intersects the Murtay River The absence

of strong individual fractitres in basin scda-

ments shark! not be taken to mean thal dis-

placement doves not occur, because strony

wurping may result From small movyeruents on

close-spaced piirallel fractures-

The recognition of structural lineaments on

photo-mosaics is made easier if the observer

fakes an oblique view of the mosaic in bright

natural light. The position of the photo-mosale

should he changed sa as to ensure thit wll

possible directions are covered. The more

tiffuse Jineamenty are easier to ste when a

number of mosaics are malched together. The

recognition. of Lineaments 3s also controlled to

some extent by the quality of the mosaics:

Some of the mosiics used in this study ire so

poor photographically and photo edges are

so dominant. that i is extremely difficult to

locate any linear features ar ol]. Alignment of

photo corners trimmed at 45° interferes with

lincamene trends to some extent, but this is a

minor matter compared to the interference of

the EW und NS trending photo edges. These

trends ate so strong, particularly whee com-

bined with processing marks in the same direc-

lion, That possible meridional (NS) ana. Jati-

tudinal (EW) lineaments aver large areas

could well be obscured.

The most prominent characternstic of struc-

tural dincaments is their persistence over great

distances through different landscapes. Many

uf the prominent lineaments shown on Fie.

7 are between 100 and 300 km in Jength, and

some exceed 400 km including Lingaments be-

longing to high frequency sets One of the

J.B FIRMAN

longest lineaments of Figs. 7 und § is thal

trending NE Fromm the NE shore of L. Gairdner

actasé the Arcoona Platea\y, | Terrens, the

Northern Flinders Ranges and Willouran

Ranges to near the NW shore of L,, Blanche

midway hetween L. Eyre and L. Frome. This

prominenc lineament matches geological boun-

daries on maps at a scale of 12250,000 in the

SW and trends am the Ste Bouguer Gravity

Map in the NE. The presence of through-

going lineyments of this kind in particular sets

of lineaments Js evidence that the lineaments

are indeed siruciurul features,

The structural lineaments do not necessarily

reflect either simple lincar lopoyraphic features

or complex alignments of topographic features,

although in many cases they parallel such

features and in some cases an: prohahty

genetically related. Throughout this work only

particular lineaments with the chatuctevistics

weady described have been recorded, Other

su'uctures prominently tisplayed on phota-

mosaics by obvious topographic features- -but

not by structural linewments—have been

deliberately omitted feom the study. ‘The struc-

ures omilled include the Eden Fault near

Adelaide, smal! meridional structures marked

by low scurps an northern Eyre Peninsula

(Miles 1952) snd the structure underlying the

Oolden Sand Range on the northern margin of

the Eucla Basin (alibough there are a number

of closely parallel lineaments in the Lest casey.

The persistence of the lineaments as straigh!

lines through different lntidscapes suggests Lhut

they are traces of planar structures with @ ver-

tical dip, Truces of such structura) features on

different mans—if followed far cnowgh—rmust

eventually reflect Ihe map projection used. but

no systematic variation from a straight fine ts

apparent on the maps produced in this stwly-

The siraightness of the lineaments ts of prac-

tical value for purposes of compilation, Where

a suspected structuri) lineyment occurs within

or alongside obviously parallel topographic

frutures, the stispected lingament can be truced

through a series of mosaics to the point where

—if it is a structural Hneament—the topo-

eraphic trends diverge and the lineament con-

linues on in the original direction. Now all

situations may be so simply resolved. Slightly

curved lineaments have been developed in the

NW and § portions of a map of the Murray

Basi) in South Australia (Firman 1970, p- 2).

In the NW these fineaments probably refiect

bedding trends in folded Cambrian Kanmantoo

Group metusediments beneath w thm veneer

STRUCTURAL LINEAMENTS IN SOU'TH AUSTRALIA 157

Of basin sediments. In the south they represent

Suranded shoretine or linear dune Features,

Both may be straight line features in part. An

important point is that it is onty when the

lineaments are compiled on a number af photo-

Mosaics that long-distance trends can be

appreciated.

The general trend of the lineaments is NE

and NW, but there arc several serfs, and rhese

intersect to form rectangular and rhomboid

blocks. The presence of structures with these

trends has long beet proposed as a result of

studies of lopographic patterns (Umbarove

1947, pp, 294-296; Hills 1956). The presence

of similar but less obvious strictures with

meridional (NS) and latitudinal (EW) trends

has also been proposed from studies of tepo-

giaphic patlerns, but these were not thought

to be us important as the others by eastier

investigniors, In this study, meridional (NS)

lineaments have been drawn on « few photo-

mosaics showing parts of the Musgrave Block,

and the Flinders Ranges, F.atitudinal (EW)

lingamentis have been drawn on. individual

photo-mosaies of the Officer Basin. the area

hear Cook in the Euela Basin, the grea pear

lake Gairdner on the Gawler Block, and

ureas near Innamincka in the Great Artesian

Basin and on the southern margin of the

Wiliyama Block. Neither the meridional (NS)

nor the latitudinal (EW) lineaments have been

continuous enough to retain on the generalised

maps accompanying this report, One reason

could he that the lineaments are not con.

tinuous, but it is more likely that their omis-

sion is connected with certain features of the

mosuics themselves, as already noted.

Methods of Compilation

Various methods of compilation were used

as the study proceeded, These are now des-

cribed in the original order of their develop-

ment. Areas involved are shown on the study

area diagram (Pig. 2).

Marrav Buxin

During the prepyration of a structural linea-

meént mup of the Murray Basin it South Aus-

tralia (Firman t970), photo-mosaics at

1:63.360 scale Were taken st random from the

set of 12 covering each 1:250,000 map sheer

Lincamenty were drawn and those which con-

tiqued across at least two of the b:63,360

scale photo-mnsaics were then transferred ta n

base map.

Some spparent off-setting appeared at mtup

borders where ane lingament in set of parallel

lIneaments was selected Tuther than another.

This produced a pseudo ea echelon efcet

which was eliminated by tracing one strung

and continuous lidieament Unrouzhoul and

abatidoniig the others, There were, bowever,

zones comprised of parallel close-spaced linea-

ments which were well defined and continuous.

An attempt was made in this case to map

more than one lingament so as to portray the

zone, Pigure 3 results from this method.

Prelindaary Stateovide Study

The coincidence of regional trends and of

specific lineamenis with faults and with other

trends on aeromagnetic maps in the Murray

Busin study was sufficiently cncouragiis to

extend the work to the rest of the State. The

size of such a projeci—the whole State is

covered by about 280 one-mile meosates, mclud-

ing about 79 in the Murray Basin—led to the

division OF that part of the State outside the

Murray Basin into five wreas on cach of which

lineaments were mapped by about eight in-

dividuals. «A total of 192 man-hours was

required Io complete the task,

Individuals new to this work were shown

structural lineaments on a mosaie selected at

random und they then delineated the lines-

ments on other mosaics selected at random

from those within the zone. The result was a

(iscontinupus pattern of lineaments huving

stmilar trends, but with major interruptions

along the mosaic howndarics, Reexamination

of the mosaics showed « number of reasons

for the discontinuily. Some individuals found

the recognition of lineaments very difficult and

they developed a pattern purallel to the linear

trends of obvious topographic features, The

trends identified in this way were either dis-

conlinuvus ar not exactly aligned with trends

of structural lineantents on adjoining mosaics.

These dilferences sufficed to climmate the non-

aligned topographic linenments during Jater

generalisation, The majority of individuals

conld sec the structural limejments, In this

case, the number of lineaments mapped

depended upon the observers confidence, Some

observers. the mure confident, having identi-

fied w lineament proceeded to delineate all the

parallel lineaments in that set appearing on

the mosaic, Others, the less confident or more

cautions, delineated only the strongest ane

more obvious lineaments. An example of this

phase of the work is shown on Fig. 4.

Although the pattern of Hpeaments on each

musiic was itself useful, the overall discan-

linuity of the State-wide pattern was a proh-

158 J, B, FIRMAN

NORTHERN TERRITORY a

= Ss

NSLAND

QUE:

}

thd

HAW Vy

WEW SOUTH WALES

Ke Fort Auuisto

Pant Lineeln

WILOMETRES FiG.9 |

73-878 bel se

Fig. 2. Study area diagram.

lem. This was overcome by a simple generalisa- Murray Basin north to the Great Artesian

tion as later described. Basin along the eastern houndary of the State.

; . The compilation began in the south in a zone

Great Artesian Basin of overlap one photo-mosaic across from north

A deliberate attempt was made to map all to south, and lineaments were then followed

the lineaments appearing on the photo-mosaics {o the north through successive mosaics. Dur-

continuously across adjacent photo-mosaic ing this phase of the work, each mosaic was

boundaries in an area extending from the checked in an altempt to locate prominent

STRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA

MARGIN OF

MURRAY BASIN

} be

i PINNAROO ‘sx:

LAN ~f

ian

Sy Kangaores

2" Island

N a

ROSE DIAGRAM

Fram Y3°SN bo S848

REFERENCE

J %,

Lineament.__ . : Ne” Nar

“

Bedding trend

Mapped fault. | _—

Geological boundary —~ -——~

KILOMETRES

J Firman

Fig. 3. Murray Basin—Structural lineaments.

acoorte

a \

Bordertown

VICTORIA

J. B. FIRMAN

TOTAL STATE

LINEAMENTS

KILOMETRES

25 50 75 100

400 290 0 2706 400 600

ROSE DIAGRAM

73—426 = Dal.WJI.E. J.8 Firman $.4 Dept. of Mines

Fig. 4. State-wide study—Structural lineaments from photo-mosaics.

SCRUCTURAL LINEAMENTS IN SOUTH

PANDIE PANDIE

CORDILLO

INNAMINGRA

—

= -

GALLABONGA

. Z, ' es Wogey e =

STRUCTURAL LINEAMENTS STRUCTURA

RANDOM MAPPING

LOCALITY MAP

Pethians ot PRIS |asentense

woteh ws ttruchial |nouments

Fofhons gl ERIE lirsampety

werolel op srcwral | noaments

Fig. 5, Great Artesian Basin. Comparison of ERTS lineaments and structural

L LINEAMENTS

CONTINUGUS MAPPING

we ERIS Lacomants Harvey fume trewds KG

Cr oathechuinl inetmency

AUSTRALIA 161

CORGILLO

INHAMINCKA

STRZELECKI

CALLABONNA

a —¥

ERTS. LINEAMENTS

ERTS licens nor watch tae

steun Kigl le oanerns

KILOMETRES,

HW «640 er

Ab Desk zl Mines

lineaments (right and

centre). Areas drawn by different methods and integrated on Figure 7 (left aid centre).

lineaments not appearing on mosaics previously

examined to the south. Such lineaments were

then mapped along with the others.

The attempt to trace lincaments continuously

removed the artificial break produced along

the EW trending margins of one-mile mosaics,

but did not entirely remove the artificial break

along the NS trending margins. This was

muinly due to the difficulty of recognising con-

tinuation of lineaments intersecting the

shorter NS trending side of the mosaic at a

small angle. The problem was resolved for

the Eucla Basin (later described), Although

the method was successful, in that a relatively

uninterrupted pattern of lineaments was pro-

duced, it had the disadvantage common to all

methods using only one observer, That is,

some lineaments not forming part of the

dominant pattern recognised in the region were

overlooked.

The contrast between the pattern of linca-

mehts derived by this method and that derived

by the earlier method involving random selec-

tion of mosaics and delineation of Jineaments

by a number of observers is shown on Fig: 5.

The procedure tor generalising structural

142

lincaments—Inter described—suceessfully Te-

moves the contrast. The actual integration of

jhe two rather different patterns is shown by

4 comparison of lineaments un the strip maps

of Fig, 5 along longitude 139°30" with the

lineaments For the same unsa shown on Fig.

Because all the lineaments were drawn and

then the number zeduced systematically with

reduction in seule, the spacing of the linca-

ments on the map prepared by the author is

meaningful, Becwuse the liicalnents on this

map integrate with the lineaments on the rather

diferent map prepared by students on adjwin-

ing areas, the spacing of lineaments on the

students nip ts also meavingful at a scale ol

1:5.000.000. A comparison of the lengths of

prominent lineaments with the lengths of

matching structures {see later) suggests that

the lengths of the lineaments derived hy this

generalisation are also meanimylul.

A check has been made om an aren in the

NE of the State where a large number of linea-

mans have been drawn independently on

ERTS imagery by Devine? ant on photo-

niasaics by the author (Fig. 3). The correspon-

dence of some lineaments is su close that they

uppear to be the same features on the ground

ideniiied hy the two different methods. Many

of the lineaments are noi related and i) seems

thal they may represent quite different Features

on the ground, Although different patterns of

lineaments have been delineated by different

observers using ERTS imagery, this is not the

reason for the difference between the linea-

iments drawn by Devine and the author. Per-

haps some kinds of lincuments can only be

identified om photo maps of large areas such

as those compilcu from ERTS imagery. Again.

different methods und different altitudes of

cumetas und scanners may reveal different

features.

Other important Teferences relating to lhe

study of ERTS jmwgery in South Ausirslia are

given in Thomson (1974)*4

Eucla Basti

A large area ineluding ihe castern Eucla

Basin and the western margin of the Gawler

Hlnck had not previously been studied hecause

phote-mosaics were not available. In this area.

5 B, PIRMAN

lineaments were identified on two blocks at

adjoining photo-mosaics with an irregular east-

west houndary close to 31°S latitude. The

Mosaics in each block were arranged for best

fit at cde centres, Despite some obvious off-

setting duc to lack of control on each mosaic

the jireaments could be traced through adjoin-

ing photo-masaics without interruption.

This method had the advantage that the

more prominent and continuguy lingaments

coulkl be readily identified. Furthermore, com-

pilylion time was markedly reduced. Apart

from the disadvantages which arise when only

one observer does the work, such as omission

ef some less obvious linvaments, there was

(nother unusual result. Because some of the

liieaments were more prominent in each block

an exuggerated zone of discontinuity was

developed between the blocks, This was re-

moved hy checking to see if lineaments

developed on one block did in Fact continue

on the other. This revealed that the differences

had been exaggerated ond that this could be

corrected by continuing the less obvious trends

from one Block of photo-mosuics to the other.

Fig. 6 shows the pattern of lincaments resulting

from the use of this method.

The excreise does show the need for check-

ing so that only real differences in the pattern

af lincaments are recorded, The presence of

regional differences in the pattern of lineaments

is important and is mentioned below,

In buill-up reas, structural linaaments are

obscured and may be difficult to separate from

engineering structures with Jinear trends. Th

these arcas. the methods of laying down a large

number of photo-masuyics has obvious aclvan-

tages. The most Important is that structural

lincatnents cum be identified outside the buill-

up area and then traced through it, The

method has alsa been proved useful on coastal

Margins, particularly where a confused paltern

of yoitueer seolian and transitional depasils

occurs together with the structural lincaments.

Gerrralivation @) Structural Lineaments

The patterns of lincaments drawn for local

areas were added to the State lineament map

compiled by the author and others at a scale

of 131,000,000, Lineaments for small areas

previously omilled for a wamely of reasons

2 Devine, S. B. 11973)—Studies in small-scale geological mapping, South Australia (Corridor +;

Cooper Basin). FRTS-| Type II Report. July [972 to January 1973. Dept. Mines S.A. Report 73/67

{unpubl.},

$"Phomson, B, FP, (1974),—ERTS-1 Imagery and small-scale mapping studies in South Australia. Final

Repart, Dept. Mines S.A. NASA final report (Type ily. DM [097/72 (unpubl, )

163

SFRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA

‘\

MAURICE

BIGHT

GREAT AUSTRALIAN

ROSE DIAGRAM

KILOMETRES

of Mines

S.A. Dep)

J B-Farmon

73-598 Del CES

Fig, 6. Eucla Basin—Structural lineaments.

\64

were also added al this stage. The largest of

these was a N& inending strip of photo-musnics

on the Western margin of the Great Aricsian

Basin, incliding Irwin, Ungoolatanna, Granite

Powns, Yoolpertunna, Marla, Ouldburra and

Manya. The method wsed fur this area was that

of continuous mapping as developed in the

Great Artesian Basin,

The procedure for generalising structural

lineaments was as follows. The 1;1,000,.000

scile compilation was first Teduced = ta

1:2,500,000 and work was begun on those

parts of this map drawn from the preliminary

State map. That is, (he parts showing greatest

discontinuity across photo-mosaic boundaries.

The continuation of aligned but disconnected

lincumients could best be seen within “ree|yngu-

lar” areas of about 2° on the side. No attempt

Was made to connect lincaments thal were

not jligned at thé original scale of 1:1,000,00,

thal te Were further apart than 0.5 km when

the lineaments were projected. Thterpolation

hetween aligned lineaments was curred oul

within each rectangle wherever the distance

apart was nO greater than the sutn of the

lengins of the aligned lincarents, This restric-

tion was necessary to avoid interpolation

across areas where it was likely that the linea-

ments did not in fact occur,

Al thes punt ia the procedure, lineaments

developed on the [nela Basin, Great Artesian

Basin und Murray Busin compilations by other

methous could he integrated because some

were aligned and continued across the boun-

tlanes of the different map areas, and because

others were of abont the same length and spac-

ing, The map wis then reduced to 1:5,000,000

and the more prominent lineaments were iden-

lifed and marked, ingluding those in local

areus delineated originally by a variety of

methads. “This pattern of lineaments is shown

on Fig. 7

‘The reality of the prominent Hueanents us

to trend. length and spacing throughout the

State Ucrives from the original attempt by the

author 10 trace all visible ineaments in certztin

areas throughout their length, and depends

upon the methes! uf generalisation used. and

upon the jotegration of the prominent lnea-

ments so defined with lineaments ofiginally

mapped it a random way by a number of

ulher observers. A comparison of prominent

lineaments and known faults shown on geo-

logical maps at the same scale shows that the

Prominent lineaments are of ~abour the same

length as the major faults. At this sesle

J. B. FIRMAN

(172,500,000) the major faults have been

traced to their natural liniits, Lincaments of

preater length could he drawn by continuing

the generalisation step by step with reduction

in scale. WW is probable that lincaments so

drawn would no Jonver ork simple faults

but would mark more complicated tectonic:

features of another order.

The venerylisajion of structural lineaments

and selection of the more continuous leads to

the omission of some discontinuous but pro-

mincnt lineaments which are possibly of con-

siderable local importance. These, however, are

Tecerded on the original mosaics at a useful

scale of 1:63,360. Ii contrast to more general

methods, those used herem make the closer

investigation of interesting local areas ut o

larger scale q rélatively simple matter

Discussion of structural lineaments through-

out the State can be simplified if the sets are

assumed to belong to conjugate systems of

intersecting lineaments with an inferred

meridional axis, as suggested by inspection of

Fig. 7, Described in this way, the lineaments

atc grouped into a system with a large

merigionyl component in which sets trend

approximately NNW and NNE, a system

with sels Lrending upproximately NW and NE,

and a system with a large latitudinal com-

ponent in which sets trend approximately

WNW und ENE. The system with a large

latitudinal component contains few lineaments

and is therefore not as obvious os the other

syslemns.

The set of lineaments in the svstem with 1

large meridional component which trends

approximately NNW is prominent in the

southern Eucla Basin, south-east Cireut Amesiat

Basin and Murray Basin, The set of linea-

ments in this system Which trends approxi-

mately NNE is prominent in part at least of

ull the Provinces. Neither the NNW nor the

NNE trending sets of lineaments are prominent

in the Musgrave and Gawler Blocks, In the

system with sels of lineaments trending

approcmatcly NW and NE. the Jineaments

of hoth sets mre prominent throughout the

State. In the system with a large latitactinal

camponent, the set of Imeaments trending

wpproximately WNW is prominent in the west

of the State, purticularly in the Officer and

Eucla Basins, but ig not sa prominent in the

easlern basins. The set of ilneaments in this

system which trends BNE occurs in all blocks

and. basins throughoot the State, and is well

developed in the Eucla Basin.

STRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA 165

NORTHERY =

”.

& eS

oP, SPs NN

OPS x

“<

anes

. as i

% Godr, ta a Sy

* “

ts re poate.

Mole Gridh tép-esent:

1 250.000 sheet oneos

RILOOMETPES

73-539 bel cee

JB Fine

(Por! Lineal

BA Depuslinusl <hr

Fig. 7. Prominent structural lineamenis in South Austrubia.

The above comments derive from a careful

inspection of the lineaments themselves. The

rose diagrams ucompanying maps of various

areas da not reveal this kind of detail, Dia-

grams of jineaments drawn by other observers

cun be excluded because frequency and trend

is biased hy artificial discontinuity at mosaic

boundaries, Other rose diagrams on maps

drawn by the author of various parts of the

State do not show the same areas as the

morpholithological subdivisions. On the mup

of prominent lineaments. longer linearments

16a

inc! sets Of lineaments in certain subdivisions

Made obvious because of strongly contrasting

trends ure not reyealed by the diagrams.

Comparison with other Features

During the Murray Basin. study, stractural

lineuments were compared with known faults,

basement trertds, and other trends derived Fram

acromagnetic mups compiled by the S.A.

Depariment of Mines und Geological Survey.

The coincidence of these features was sur-

prisingly close. For example, structural linea-

ments und aeromagnetic trends marking the

western edge of the Murray Wasin all fell

upon a major “hardrock” boundary originally

delinented hy B. P. Thomson (unpub) (sec

Firman 1970, p. 2, and Fig. 3 of this report),

Crealogical

The 125,000,000 cumpilation showing the

mote prominent structural lineaments was com-

pared with geotogical and geophysical maps.

The purpose of this comparison was to chech

the amount of coincidence at various scales of

the patterns and trends of structural lines-

ments with the pallerns and trends shown on

other geeluvical and geophysical maps,

A comparison of the structural lincaments

with snll-seale maps showed only a general

agrecmem of patlerns and trends. A check

of che Stite geological 1710,000,000 map with

other ycologicul maps at about this scale

showed gross diiferences in geological pattern

for the some area, due no doubt to the extreme

simplification of outcrop boundaries concomi-

tant with weological interpretation on maps al

this scale. For this reason, a close fil with

general mops of this kind could not he

expected.

The agreement between structural Jinen-

ments and large scale maps was mitch better.

A comparison leading ta selection of major

lincaments has been made with features on the

Tectunic Map of Australia and New Guinean

(1971) at a scale of 125,000,000. A. compari-

son of strectural lineaments with all the avail-

able regional geological maps at a scale of

1:250.000 showed by far the best match of

structural lineaments with geological patterns

und trends.

Structural lineaments thal match the tectonic

amd regional geological maps are shown on

Fig. &, ‘This match could probably be improved

by the omission of those parts of the linea

ments ealending beyond the region wherein

the fic is best. Although this work could not

provide » complete structoral map becuse of

J, B FIRMAN

the restriction of features delinealed to the

pirliculur lineaments discussed herein, 1 large

number of important structures are in fact

iWentified.

B. G. Forhes has suggested (pers. comm,)

thul areas of different density of lineaments

require explanation. It could be arued that

some of the areas of sparse Hneaments ure

due to a cover of surficial deposits, but ib is

ihe author's experience that the lineaments are

guite well displayed upon photo-mosiics of

leriain veneered by such deposits. An <xplana-

tion of the OMeer-Eucla Basin atea of sparse

lineaments surrounded by u zone of greater

density of lines is that there i¢ a well developed

zone of lincaments marginal ta the adjoining

Musgrave and Gawler Blocks. No such

explanation can be made for the zone of

greater density of lincaments trending ENE

through the Conper Basin (see Fig. 8),

There are numerous N-S and F-W tending

features on the tectonic and regional gealogi-

cal mups for which there are no corresponding

structural linéaments, probably for the reasins

already outlined. Given that the close fit

between features on the different kinds of maps

is real, a Case could be made fur a final phase

in this kind of study ta which the eriginal

Mosaics were again examined to locate why

importunt lineaments oniitted during general-

isatton. A re-examinatiin of the ofiginal

mosaics or detailed mups could also be made

to check for lineaments with un even better

fit than those selected from the generalised

maps,

Te does scem thal separate investigations oF

the fir of structural lineaments with other

geoloxical patterns and wends could he

eliminated if the lincaments were mapped

along with other detailed ecological features at

an curly stage in regional mapping.

Geophysical

Three kinds of geophysical maps have been

compared with the maps of structural linei-

ments. These are the Bouguer gravity map of

the Stue (Coppin, Hall & Milton 1971}, the

map of the Great Ariesian Basin province

showing contours of magnetic intensity and

interpreted depths to magnetic basement

(Coppin & Hall 1972), both ac a scale of

121,000,000, and the 1:250.000 and £:63,360

aeromagnetic maps used in the original study

of the Murray Basin in South Australia.

Although some of the following comments

are based pon the companson of structural

linewsients With all the geophysical maps men-

STRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA 167

TERRI AY,

—

MUSGRAVE tf &

2 Orricen

HastN

Lirecinverts nites nailing eeag

cr osoy peietlel te,

fealurus mi tha WF Tron Mog

lineaments edhe avgned wile teehee Inalins,

or Hlhag the parerr

nih He V2) estos May. -=jf

lineaments wolchie, qeulugicul bevader nes

oh bPSGQGN qrups 2,

Linewnwnts meteh ina trends an the

Bite Bowguer gravity ope,

Crystalline Sasewent

Bewidanes of tns'ays

Linds of sedineniation cuciog sptrified mie inleiwala — -v

Eloseu pastivc Beuel olavity asdmalies

“vk

Th. ARTERIAN

*. *

Sf 1

Penn }

BLOGK 4,

sollént features ony

Por deluits, see the

Teclonic Mep of Auatia ic

and Mew Grinea te? |

KILOMETRES 500

SS el bee

Sh Dew ol Moves

Fig. 8. Structural lineaments matching geological und geophysical patterns and trends,

lioned, oly the Bouguer gravity map with

complete Siate coverage has been used to cam-

pile the appropriate lineaments on Fig. 8.

The Bouguer gravity map docs show similar

trends, but selection of coincident features is

not easy because a number of contour lines

are shown rather than single features, which

on checking can be shown to be either cainci-

dent or not coin¢gident with a particular linea-

ment. There are two kinds of geophysical

features on the gravity plan parallel to linea-

ments. These are gravity contour shapes which

168

J, B. FIRMAN

KILOMETRES

you

}OXTON BASIN

Mesownic sediments

Dijedtian of ice wovement

Pera Sentinels

DELAMERIAN GRANITE

Bediack outcrops. Including

Fo aeozolc granite (diagrammatic)

Centedes ef eeorent thickress of

Cambrian yes ae the le of fést

below bese BRUNA A FORMATION _

Fe 507 B Firmen SA Cust) of Mies

oy Say

jBardenlown

‘ "

Cembian sedinems of the

KANMASTOQ TROUGH

Cambriag Shell Zone

Prelerozere sediments of the

ADE AIDE GIOSYNG LINE

Precambrian STUART SHELF.

Norther linn) of Cretoceous sediments

in the Gambier Emboyment — — apap pepe

Foul —

lineament. —.,

MURRAY BASIN Tertary prargin

Cartaurs oh tie Tertiary too

Dapths beraw sea—leve! in feel,

Stbmorine form | res ar fathers 2 0 se

Fig. 9, Murray Basin. Development of the western margin and geology of the

Tertiary floor.

STRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA

RECENT

Aeolion gypsum sond

Coengmbidgal Fm. eos

Molingoux Sand

Bunyip Sand .__, .

Lineoment —~_ __

73—544 Del. WIE.

we |

i oe d Fe ieee

~ RINNAROO BLOCK ~~

KILOMETRES

20 3002S AO

LEGEND

PLEISTOCENE

Gre Loveday Soil

Woorinen Fm.

Bokata Soil

Blanchetown Clay __

TERTIARY

sso

Undifferentiated $

Aeromagnetic trend lines

Form fine—Loxton Basin

Contour of Tertiary

Floor Depth below sea ps

level in feet-~

I.B.Firman 5.A, Dépt. al Mines

Fig. 10. Tectonic sketch on RENMARK shect S1/54-10.

(70

in detail fit fairly closely io shapes formed by

intersecting lineaments—this fit may be rather

more apparent than real, because selection of

another contour interval could produce it

rather poor fit—and major trends on the

atavity map which parallel major trends on the

map of structural lineaments. In some places

small closed features on the gravity map are

marked by the intersection of several linea-

ments or are framed by a pattern of lincuments

around the periphery of the feature,

On the 121,000,000 geophysical map show-

ing contours of magnetic intensily and inter-

preted depths to mignetic basement, the fit of

structural lineainents with geophysical features

is nor good, The trend of structural lincaments

cuincides best of all with the trend of contours

showing depths to magnetic basement: There is

a very poor fit of the trends of structural

lincaments and trends of contours of total

marmetic inleasily, except where the Irends at

contours of depths to magnetic busemeot and

af contours of total magnetic intensity are in a

similar direction. Only a few of the structural

lincaments are coincident with inferred base-

ment! faults shown on the geophysical map,

Aeromagnetic maps at a scale of 1263.360

were used to compile trends of geromuynetic

features in the Murray Basin. Structural linea-

ments Were in very good agreement with yero-

mughetic trends on this map {Firman 1970,

p. 2),

The comparison of maps af structural linca-

ments with other geological and geophysical

maps shows sufficient correspondence of pat-

terns and trevids to confirm the earlier con-

clusion from the Murray Basin study that the

linear features on photo-mosaics are jctitully

structural features. Muny of the lincaments

mark structures associated with warping of the

basins and uplifting of the ranges. and refiect

profound structures and tectonic elements in

the crystalline basement.

An incidental observation resulting from this

study is that the sélection of more important

atroctural lineaments. cun best he made by

comparison with olher geological and yea-

physical features associated with the linca-

ments, Firman (1972, RENMARK sheet) and

Fig, 9. und the tectonic sketch in Firman

(1972) together with Fig, 10, provide

examples

J. B. FIRMAN

‘Time of Origin of Structural Lineaments

in general, structural lineaments appear to

post-date very young deposits. This is. con-

clusion based upon their presence in arcus

mantled by surficial deposits thick enough fo

bury the older rocks. Some of the lineaments

serve to outline the margins of Busing con-

taining relatively flat-lying Cainozoic, Meso-

zole und Palaeozoic rocks and these lineaments

could mark much older rejuvenated structures

as ald us the first deformation of the original

basins,

In regions of strangly folded Palaeozoic and

older rocks, the lineaments are cross-cutting

with respect to majer fold (rends and obviously

post-date them. However, mujar structural

boundaries between the fold belts and adjoin-

ing blocks of crystalline hasement are also

miucked by structural lineaments, The implicu-

tion i8 that the lineaments mark much older

structures, some of which must immediately

posi-date the welding of ancient sedimentary

unl metamorphic components te form the

blocks themselves.

Because both the oklest structures delimeal-

ing basement blocks and the youngest Jinea-

ments form part of the same through-going

and nhiquitous sets of structural lineaments,

it appears that there has been no major dis-

orientation within the study area of even the

oldest structures.

Acknowledgements

This report is published with the approvul

of the Director, $A, Department of Mines.

A number of student and graduate geologists

assisted! the writer in the compilation ot the

preliminary State-wide study, including R, F

Boomsma. R. Coumb, BE. H. Briese, G. Griffin,

Thinks are duc to Mr. B. P. Thomson and

Dr. B. G. Forbes for helpful discussion during

Phelo-interpretation of the lineaments.

Lineament trends were measured hy M. Cal-

well und Bo Savage of the computing group

in the Exploration Geophysics Section, and

rose diagrams were prepared by $. Cummings

and W. Jeffery of Cartographic Compilation

Section.

The ilfustrations accompanying this paper

were prepared by the Illustrating and Display

Section under the supervision of B. F. Frost.

STRUCTURAL LINEAMENTS IN SOUTH AUSTRALIA 17i

References

B.M.R. (1960).—Tectonic map of Australia

1:2,534,400. (Bureau of Mineral Resources,

Geology and Geophysics: Canberra.)

Corrin, R. J., & Hari, J, M. (1972)—Great

Artesian Basin in South Australia. Contours

of mugnetic intensity and interpreted depths

{o magnetic basement (scale 1:1,000,000).

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

Coppin, R. J., Hatt, J. McG.. & Mitton, B. E.

(1971).—Great Artesian Basin in South Aus-

tralia. Bouguer gravity anomaly map (scale

1:1,000.000), (Geol. Surv. S. Aust-: Ade-

laide,)

Dennis, J. G. (Ed.) (1967),—International Tec-

tonic Dictionary. Mem. Am, Ass. Petrol,

Geal. 7.

Firman, J. B. (1969)—An introduction to the

structure and stratigraphy of the Murray

Basin and the Gambier Embayment. Jn B.

Daily (Ed.), “Geological Excursions Hand-

book”, 41-48, ANZAAS, section 3, 1969.

Firman. J. B. (1970),—Structural lineaments in

the Mutray Basin of South Australia. Quart.

geal. Notes, geol. Surv, §. Aust. 35, 1-3.

Firman, J. B. (1972) —RENMARK South Aus-

tralia. Explanatory Notes 1:250,000 Geologi-

cal Series Sheet S1/54-10 International Index.

(Geol. Sury. S. Aust.: Adelaide.)

Firman, J. B. (1973).—South Australia, Jn R. W.

Fairbridge (Ed,), “Encyclopedia of World

Geology”, (Reinhold: New York.)

Forres, B. G., Coats, R. P., Weas, B. P., & Hor-

wirz, R. C. (1965).—MARREE map sheet

H54-5, Geological Atlas of South Australia,

1:250,000 series. (Geol. Surv. S. Aust:

Adelaide.)

Freyrac, J. B., HEATH, G. R., & Worrner, H.

(1967,)—OODNADATTA map sheet

$G53-15, Geological Atlas of South Australia,

(:250,000 series. (Geol. Surv. S, Aust,; Ade-

Taide.)

G.S.A. (1971).—Tectonic map of Australia and

ew Guinea 135,000,000. (Geological

Society of Australia: Sydney.)

Hirts, E, 8. (1956).—A contribution to the

morphotectonics of Australia. J. geol. Soc.

Aust, 3, 1-15.

Hoses, W. H. (1911).—Repeating patterns in the

relief and structure of the land. Bull. Geol,

Soc. Am. 22, 123,

Mi.es, K, R. (1952).—Tettiary faulting in north-

eastern Eyre Peninsula, South Australia.

Trans. R. Soc, S. Aust. 75, 89-90,

SpricG, R. C. (1952)—The Geology of the South-

East Province, South Australia, with special

reference to Quaternary coastline migrations

and modern beach developments. Bull, Geol.

Surv. §. Aust. 29.

Umocrovr, I. H. F, (1947),—The Pulse of the

Earth. (Martinus Nijhoff: The Hague, )

Witttams, A, F. (1973)—GASON map sheet

$G54-13, Geological Atlas of South Australia,

1:250.000 series (Geol, Surv. S. Aust.: Ade-

laide.) (In preparation.)

VOL. 98, PART 4 30 NOVEMBER, 1974

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Orchard, A. E. A New Species of A SOR ney, GiialothpAceas) from Northern

Australia - - - = - - - - 173

Hutton, J. T. Chemical Characterization and Weathering Changes in Holocene

Volcanic Ash in Soils near Mount Gambier, South Australia - 179

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

Stromatolites. Part III - - = - - - - - 185

Houston, T. F. Amphibolurus gibba, a New Dragon Lizard (Lacertilia:

Agamidae) from Northern South Australia - - - - 209

van Tets, G. F. A Revision of the Fossil Megapodiidae (Aves), ia a

Description of a New Species of Progura De Vis - - 213

van Tets, G. F., & Smith, Meredith J. Small Fossil Vertebrates from Victoria

Cave, Naracoorte, South Australia III. Birds (Aves) - - 225

van Tets, G. F. Fossil Birds (Aves) from Weekes Cave, Nullarbor Plain, South

Australia - - - - - - - ~ - - 229

Annual Report of Council, 1973-74 - - - = - - - - - 231

Award of the Sir Joseph Verco Medal - - - - ~ - - - 232

Balance Sheet - - - - - ~ - - - - - - 233

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

A NEW SPECIES OF MYRIOPHYLLUM (HALORAGACEAE)

FROM NORTHERN AUSTRALIA

BY A. E. ORCHARD*

Summary

ORCHARD, A. E. (1974).- A new species of Myriophyllum (Haloragaceae) from Northern

Australia. Trans. R. Soc. S. Aust. 98 (4), 173-177, 30 November, 1974.

A new species, Myriophvllum callitrichoides, is described from northern Australia. It differs from

all previously described species in its dimorphic stems and leaves, filiform styles and cruciform

fruit, and seems to have no close allies. It is tentatively placed near M. integrifolium Hook.f. and

M. drummondii Benth.

A NEW SPECIES OF MYRIOPHYLLUM (HALORAGACEAE)

FROM NORTHERN AUSTRALIA

by A. E. Orcnarn®

Summary

OrcHAko. A. E. (1974).—A new species of Myriaphylium (Haloragaceae) ftom Northern

Australia. Tranny KR. Sec. S. clus 98 (4), 173-177. 30 November, 1974.

A new species, Myrigphythin calliiriehoides, is deseribed trom northern Australia. Tt

differs frum all previously desevibed species in its dimorphic stems and leaves, filiform: styles

unl eroviform fruit, and seems ta have no close alfies. In is tentatively pluced near M. integri-

folinm Hook t. and Af. denmunoendii Benth.

Myriophylam callitrichoides: Orchard, sp, nov

Herbu aquatica ad 25 em alta, caules. et fotia

dimorpha. Cuules primarit moverute robustt ascen-

dens ad basin radicuntes 5-7 em alti 2-4 mm clia-

mots spars Famost, Colla alterna obovoidea (in

vivo) vel spathulata (in siceo) 6-8 mm longa

1.52.0 mm Tata apicum versus contracta: ad 1,0

mm busin versus suceulenta integra, apices rotun-

dat cullo atruto priediti, plusminusve recurvata

glandibus 2 minutis fliformibus stipuloidibus udeei-

duis atralis subleola. Caules secundarii filiformes

axillis foliovum inferiorvis exarientes, ad 1S civ

longi 0.2-0.3 mo diametris., axillis foliorum 1.0-

L5 mm Jongorum distantiim wlternorum = (raro

suboppesitorun) redlctorim bractegidum ramifi-

cuntes, Polit emergentia ad extremum eaulium

secuntariorum urete agegregata alterna petiolata.

lubiina succulenla ovata 2.0-3.5 nim longa 2.0-2.5

mn latit integra, apex rotundatus callo atro api-

cali. basis contraeta abrupte ad petiolum, nervi

indistincli plusminusve paralleli, peliolus 1,0-1.5

mm longus, oppendicibus stipuloidibus 2-4 atris

filiformibus aa basion petiolorim, ususquisque

folium emergens florem unum bisexuiem wdoulum

ad petriolluim: praeditus

Florey 4-meri sessiles appendicibus 2 stipuloidi-

bus subtenti. Sepala 4 anguste deltoidea (.2 mm

longa O.1 mm tata integra vel infirrne denticulata,

Petula 4 cuculara 0.8-1.0 mm longa 0.3 mm tata

infirme curinata, Stamita 4 antipetala fila OQ mm

longa ad ca 0.5 fm pest unthesin protenti,

imtherue luteue ovoideae 0.6 mm longae 0.2-0.3

mm latae minule apiculatae. Styli 4 filiformes 1.5

mm longi. Qyarium sessile obturbinatum 0,4-0,5

mm longhm 0.7-0,8 mm latum sub petalis sacca-

tim sub sepalis suleatum 4-loculare ovalis unis tn

WrUsguisgie,

Proctus cruciformis petiolus yaricus, mericarpia

ad apices connata deorsiim extrinsecusque ad angu-

lum 45° divergentia unwuste obovoidea .t-{.2

mm longa 03-04 mm diametro verrucosa in

superficie emMeriore praceipue in parte inferiore

tuberculis retrorsis; semen 1 i unusquisque meri-

CuTpo.

langie Creek, 132°47 ER Rockhole in

sindstone conglomerale, Aqttatic rooted in organic

Sludge: dimorphic leaves. submerged leaves fleshy.

CANB243801 (fh. fra! (Fig. 1). lsarpic AKL

DNA, NT!, BRI, K, 1,

Weak aquatic herh to 25 em high, stems und

leaves dimorphic. Primury stems moderately

robust, ascending, rooting at base, 5-7 em tall,

2-4 mm in diam.. sparsely branched, leaves

alternate, succulent, ohovoid (in vivo) or spa-

thulate (in siceo), 6-8 mm long, 1.5-2.0 mm

broad towards tip, tapering to 1.0 mim towards

buse, entire. slightly recurved, tip rounded,

with black terminal callus, Leaves with 2

minute filiform stipule-fike deciduous black

glands at base of petiole.

Filiform secondary stems atising in axils of

lower (primary) leaves. to 15 cm long, 0.2-

0.3 mm in diam,, branching from axils of dis-

tant alternate (rarely subopposite) bract-like

reduced leaves 1.0-1,5 mm long. Emergent

leaves closely clustered at tips of secondary

stems, alternate, petiolate, himina succulent.

ovate, 2.0-3.5 mm long, 2.0-2.5 mm wide.

entire, tip rounded with black apical callus.

base abruptly tapered to petiole, veins indis-

tinct, = parallel, petiole 1.0-L.5 mm long, with

2-4 black filiform, stipule-like appendages at

its hase. Each emergent leaf provided with

* Auckland Instituie & Museum, Private Bag, Auckland, New Zealand.

174 A. E, ORCHARD

YBRASIUM

SUL EEALIONDE

CAI

NO 245801

Fig. 1. The holotype of Myriophyllum callitrichoides Orchard.

A NEW SPECIES OF MYRIOPHYLLUM 175

single bisexual flower, adnate to middle of 0.8-1.0 mm long, 0.3 mm wide, weakly keeled.

petiole. Stamens 4, antipetalous, filaments 0.1 mm long,

Flowers 4-merous, + sessile, flanked by 2 lengthening to ca 0.5 mm after anthesis; anthers

stipuloid appendanges as for leaves. Sepals 4, yellow, ovoid, 0.6 mm long, 0.2-0.3 mm wide,

narrow-deltoid, 0.2 mm long, 0.1 mm wide; minutely apiculate. Styles 4, filiform, 1.5 mm

entire or weakly denticulate. Petals 4, hooded, long. Ovary + sessile, obturbinate, 0.4-0.5 mm

Figs. 2-4. Habit of M, callitrichoides, Fig. 2—Whole plant. Fig. 3.—Base of plant showing young pri-

mary stem and leaves, and lower part of secondary stems. Fig. 4.—"Rosette’” of emergent

leaves, flowers and immature fruit, viewed from above. (All from Duniop 3387: fig. 2 from

dried material, figs. 3 and 4 from liquid preserved specimens.)

(76

long, 0.7-0.8 mm wide, saccate below petals,

grooved below sepals, 4 locules with | avule in

each,

Fruit black, cruciform, straddling petiole.

mericarps fused at apices, diverging down-

wards and outwards at 45”, mericarps narrowly

obovoid, 14-1.2 mm long, 0.3-0.4 mm in

diam.. vertucose on outer fage, particularly in

lower part, with downward pointing asperities;

I] seed per mericarp.

The epithet “callitrichoides” refers to the

emergent leaves, which very closcly resemble

the rosette of floating leaves of Callitvi¢he siag-

natin.

This remarkable plant dillers [rom ull pre-

viously described Myriophylluny specics in a

number of respects. Although dimotphy of the

leaves is common in the genus, with the cmer-

A, E. ORCHARD

vent leaves. often very different from the sub-

merged ones, this scems to be the only species

that also has dimorphic stems (Fig, 2). The

primary stems (Fig. 3) are the relatively stout,

honeycombed axes common in the genus, but

the secondary stems bearing reduced, bract-like

leaves at wide intervals, and arising from the

axils. of the primary leaves, are filiform and

flexible. In contrast to the primary stems they

ure frequently branched. The emergent leuves

are borne in a tight rosette-like cluster at the

tips of the secondary stems (Fig, 4), and are

unusual in that they apparently Maat on the

surface of the water, rather than being held

aloft as in most other species, Furthermore, the

flowers are adnate to the petioles of the emer-

gent leaves, instead of being borne in their

axils (Fig. 5), The styles are filiform, instead

Figs. 5-9. Flowers aud fruit of M. callitrichoides. Fig. 5.—Flower adnate to petivle of emergent leaf-

Fig. 6.—Isolated mericarp viewed from slightly above, with positions of other mericarps

indicated, Fig. 7—Smele mericarp viewed from below. Fig. 8.—Semimature fruit with one

abortive mericarp, viewed from above. Fiz. 9.—The same, viewed from below. (All from

Hunlop 3387; fie. 5 drawn trom liquid preserved material, figs. 6-9 from dried material.)

A NEW SPECIES OF MYR/OPHYLLUM

of clavate, and more closely resemble those of

Gunnera than those of other Myriophylium

species. The fruit is unique, not only in its

peculiar radiating mericarps, but also in the

fact thal they are fused near their apices, rather

than lower down (Figs. 6-7). Occasionally |

(very rarely 2) of the mericarps fails to deve-

lop, and an irregular fruit results (Figs. 8-9).

With all of the above peculiar features, it is

difficult to place M. callitrichoides in existing

treatments of the genus. Ih the standard mono-

graph (Schindler 1905), it keys out to subgen.

Mvyriophyllam (“Eumyriophyllum”] sect, Tes-

saronia, but does not fit well into any of the

subsections. Van der Meijden (1969, extended

in van der Meijden & Caspers 1971) has

recently published a revision of the south-east

Asian, Malesian, Mascarene, and African spe-

cics of the genus, Using his key, M, ceallitri-

chojdes comes closest to M. oliganrhum (W. &

A.) F.v.M. and M. tuberculatum Roxb,, but this

reflects only leaf arrangement and the tetrao-

drous flowers; in leaf, flower and fruit mor-

phology there is little similarity.

The nearest relutives of M. callitrichoides are

probably M. integrifeliium Hook.f. and M.

drummondi Benth. with which species it

177

shares its alternate, entire leaves, tetrandrous

flowers and ovoid anthers. However. the rela-

tionship is not close, as M. callitrichoides dif-

fers from the other two species in its dimorphic

stems, broader and more succulent leaves, bi-

sexual flowers which are adnate to the petioles

of their subtending leaves, filiform styles and

cruciform fruits,

At present M. callitrichoidey is known only

from the type collection. Further specimens ate

needed to determine whether its peculiar habit

18a constant feature or merely a reflection of

ecological influences (e.g. a sudden change in

water level during the growing season). How-

ever, even if this should be shown to be true,

the species is still adequately characterized by

its flowers and fruits to merit recognition as a

most unusual member of its genus.

Acknowledgements

[ am grateful to Mr C, R. Dunlop, of the

Animal Industry and Agriculture Branch,

Department of the Northern Territory, who

first. brought this plant to my attention. The

duplicate collections in. Herbarium Austra-

liense (CANB) and the Arid Zone Research

Institute (NT) were kindly loaned by the

curators,

References

ScHInpier, A, K. (1905).—Halarrhagaceae. Das

Pflanzenreich 23, 1-133.

VAN DER Merpen, RK, (1969).—An annotated

key to the South-East Asiatic, Malesian, Mas-

carene and African species of Myriophyllum

(Haloragaceac). Blumea 17, 303-311.

VAN DER MEIJDEN, R., & CAspers, N. (1971).—

Haloragaceae. Flora Malesiunu 7, 239-263.

CHEMICAL CHARACTERIZATION AND WEATHERING CHANGES IN

HOLOCENE VOLCANIC ASH IN SOILS NEAR MOUNT GAMBIER,

SOUTH AUSTRALIA

BY J, T. HUTTON*

Summary

HUTTON, J. T. (1974).-Chemical characterization and weathering changes in Holocene volcanic

ash in soils near Mount Gambier, South Australia Trans. R. Soc. S. Aust. 98(4), 179-183,

30 November, 1974.

Surface soil samples collected within 12 km of the volcanic crater of Mt Gambier, South Australia,

have been analysed for thirteen elements by X-ray fluorescent spectrography. The amounts of eight

of these elements in each of ten samples have been compared with the amount present in a sample

collected close to the volcano and it is clear that the ejected material was of uniform composition.

The amount of ash deposited on the Pleistocene beach dune sands decreases as distance from the

Mount increases.

By comparing the present composition of the ash with the composition of a sample of Mt Gambier

basalt, it is shown that 60-80% of the calcium, magnesium and sodium has been lost but there has

been essentially no loss of titanium, silicon or aluminium. In 5,000 years, about one half of the

volcanic ash has weathered to clay minerals which do not readily disperse and the leached sodium

and magnesium appear to reach the groundwater.

CHEMICAL CHARACTERIZATION AND WEATHERING CHANGES IN

HOLOCENE VOLCANIC ASH IN SOILS NEAR MOUNT GAMBIER,

SOUTH AUSTRALIA

by J. 'T. Hurron*

Summary

Hutton, J. T. (1974)—Chemicul characterization and weathering, changes m Holocene vol-

canic ash in soils near Mount Gambier, South Australia Trans. R. Soc. S. Aust. 98(4),

179-183, 30 November. 1974.

Surface soil samples collected within 12 km of the volcanic crater of Mt Gambier, South

Australias, bave been wnalysed for thirtcen elements hy X-ray flugrescent spectrography, ‘I'he

aniounts of eight of these elements in each of ten samples have been compared with the

umouot present in a sample collected close to the volcano and it is clear that the ejected

materia! was of uniform composition, The amount of ash deposited on the Pleistocene beach-

dune Sands decreases as distunce from the Mount increases.

By comparing the present composition of the ash with the composition of a sample of

Mt Gambier basall, it is shown that 60-80% of the calctum, magnesium and sodnim has been

lost but there has been essentially no loss of titanium, silicon or aluminium, Jn 3,000 years,

about one half of the valeanic ash has weathered to clay minerals which do pot readily

disperse anid the leached sodium and magnesium appear to reach the proundwater.

Introduction

Hutton, Blackburn & Claike (1959) indi-

cated the distribution of soils affected by val-

eanic ash from Mt Gambier by a study of the

size of the particles: added to the siliceous sand

of former beach dunes. As this earlier work

had shown that ihe material ejected and depo-

sited on the existing dunes was uniform in the

physical size of the particles, it should be pos-

sible from a study of the elemental composition

of the same soils to confirm the uniform nature

of the ash and also sce what elements may have

been differentially lost by weathering since the

deposition of the ash 5,000 years ago (Fer-

gusson & Rafter 1957).

Methods of Analysis

Eleven surface samples siudied previously

were analysed for thirteen clements by X-ray

fluurescent spectrography. Fur the eight major

clements, magnesium, aluminium, silicon, phos-

phorus, potassium, calcium, titanium and iron,

the ignited soil samples were fused with a

lithium borate flux as deseribed by Norrish &

Hutton (1969) and cast into glass dises. Cali-

bratton for these elements was based on fusions

of pure chemicals in the borate flux and results

were all corrected for variations in mass ab-

sorption due to variations in sample caomposi-

tion.

For the elements chromium, manganesc,

nickel and zinc. present in low concentration

(10-1,000 ppm), and for sodium, the finely

ground samples were pressed into suitable dises

without any dilution (Norrish & Hutton 1964)

in order to obtain sufficient sensitivity, Calibra-

tion was made again by comparison with stan-

dards prepared from pure chemicals mixed with

a sample of clean quartz. Variations in mass

absorption due to changes in sample composi-

tion were measured and the appropriate cor-

reciions applied.

Results

The results of analysis of sample A 363/13,

collected about 3 km northwest of the Mt

Gambier crater and considered from field mor-

phology to have the greatest amount of ash

mixed with the leached siliceous sand, are given

in Table 1. For comparison the resujts of ana-

lysis of sample A 361/1, collected from near

= CSIRG Division of Sotls, Glen Osmond, S. Aust. 5064.

! CSIRO Division of Soils sample reference number.

180 J. T. HUTTON

TABLE |

Composition of soils, volcanic ash (calculated) and estimated change daring weathering

Soil Soil Present Sb change

lurgely largely compositian Composition (relative to

Element dune sand volcanic ash of ash* of hasaltT basalt)

AJ61/1 A363/1

Na. %e 008 0.17 0.4 wag —&0

Mg, % 0.03 1.47 24 w.12 —70

1 0.90 5.35 a0 7.62 +20

Ob 45.7 34,9 26,0 22.0) +20

Ht 0.01 0,29 0.20

a 0.22 0,59 1.3 1.27 0

a 0.07 1.04 3.1 7.A8 60

6 OAS 0.96 1.3 1,22 +20

Cr, ppm 29 118

Mn, ppm {1s B25

Fe, % 0.52 5.08 8.2 8.35 1)

Ni, ppm 2 65

Za, ppm 5 96

Scat ich

* Average of values calculated on assumption that A 363/1 contains 40% dune sand, A 4464/1 con-

tains 45% and A 349/1 contains 50%.

+ Stanley (1909).

TABLE 2

Composition of ash soils expressed ay % composition af A 363/1-

i cae eee EE Sst ESSE SEES ESSER nn

Distance

Sample Mt Gambier

number km Direction Ms Al Ti Fe Cr Mn Ni Zn

A363/1 3 NW 100 109 100 1nd 100 100 100 100

AN 464/1 24 E 91 R7 79 81 2 66 118 BS

A 349/1 3 S 83 92 7 83 &8 75 118 7

A3S1/) ft SE 46 104 54 60 67 Th 46 AR

A 364/1 5 S 56 40 66 58 57 64 50 42

A 360/1 64 N 28 53 50 47 68 a7 40 28

A 355/1 3 EK 38 36 41 38 33 43 49 pa)

A 2092/1 \J NE: # 29 39 27 3 28 16 25

ASS8/1 63 NE i 23 12 25 31 21 3 6

A 467/1 5+ NW % 20 11 12 19 21 3 7

* Amount too low to be determined with sufficient accuracy to obtain » meaningtul figure.

the northern limit of the influence of the ash,

are also given.

Of the thirteen elements determined, mag-

nesium, aluminium, titanium, iron, chromium,

manganese, nickel and zinc are considered to

be associated with volcanic ash and the results

for these elements in the other nine samples

are given in Table 2, where they are expressed

as a percentage of the concentration found in

sample A 363/1.

Discussion

The eight elements chosen for listing in

Table 2, namely magnesium, aluminium, tita-

nium, chromium, manganese, iron, nickel and

zine, ate present in higher concentration in

basultic type rocks than in other types such as

sands, limestones or granites. For this reason

they were chosen in this investigation to be In-

dicalors of material of volcanic origin in a

region of sand dunes and swales. Sample

A 361/L is typical of the surface of the sand

dunes and sample A 363/1 taken 3 km NE of

the crater of Mt Gambier is typical of the

material of volcanic origin after 5.000 years

exposure, The data in Table 1 show that the

dune sand is not pure quarlz as it appears to

contain a titanium mineral and some clay or

feldspar to account for the potassium. The

umount of potassium would indicate that wea-

thering and leaching have not been excessive

and so the Jow levels of some elements, parti-

cularly magnesium and nickel, suggest the ab-

CHEMISTRY OF VOLCANIC ASH IN SOILS NEAR MT GAMBIER

sence of volcanic ash from this site 1i km N

of Mt Garnbier,

By calculating the amount of these eight

“basaltic” elements present in the ten samples

of surface soils as a percentage of the amounts

in sample A 363/1, the significance of the dif-

ference in the composition of these soils be-

comes apparent. As distunce from the Mount

increases, 4he amount of each element is re-

duced by a similar proportion, In order to

determine the amount of ash in the soils stu-

died, relative to sample A 363/1, three some-

what independent sets of chemical data and

the particle size data given in Hutton, Black-

burn & Clarke (1959) can be used. OF the

eight elements recorded in Table 2, magnesium,

aluminium, titanium and iron are preseat in

A 363/1 at about 1% or more, They can be

determined accurately but as some variation in

asa composition can be expected, the relative

percentages given for these elements in Table 2

were averaged for listing in Table 3. Chro-

mum, manganese, nickel and zinc are present

in smaller amounts (less than 0.1%) and ure

therefore determined less accurately, but they

do represent u different geochemical parameter

from the major elements, and again, 10 reduced

individual fluctuations, the data of Table 2

were averaged for presentation in Table 3, The

third chemical measure of the amount of ash

material is obtained from the results of the

determination of the silicon content of cach

sample because the addition of the basaltic

minerals will ceduce the high silicon content of

the silica sand of the dunes. (Thts. measure is

nat strictly independent of the other chemical

values in that wher expressed as. oxides, SiO.

constitutes fhe hulk of the sample that is. noi

Al,O.. MgO, Fe,O., and TiO.+. The amount

of particles im the size range 2 ym to 50 ym

found in these same soils js given by Hutton,

Blackhurn & Clarke (195%) and the very high

ash soils close to Mt Gambier have about 40%

of these particles, Again, the amount of 2 pm

to 30 «um particles in the samples from the

other sites can be calculated relative io this

figure and the data are given in Table 3. These

four estiniates have been used ro calculate

Tmean values for the relative proportions of the

basaltic material added to the sand dines, The

comparatively low values of standard devia-

tion (Table 3) suggest that ial! four measures

are of the one property.

The sumples examined in this study had

mostly been collected from soil profiles asso-

ciated with the higher sand dunes, where some

mixture of ash und sand has occurred, The data

given by Flutton, Blackburn & Clarke (1959)

had indicated that in many cases the resulting

mixture is unifarm down to 40 em. This mix-

ing is nor due to cultivation as many of the

simples were collected from roadside cuttings,

but is attributed to the activities of soil animals

in fertile, well-aggregated soils. Evidence sug-

gests that where more than 150 cm of ash Was

deposited there was less mixing of sand and

ash, while as the deposit of ash became thinner

more mixing and resultant dilution took place.

Hence it is difficult to define the true limit of

the area that received the voleanic accession,

The climate of Mt Gambier. with the aver-

ige Maximum temperature ranging [rom 12°C

to 25°C and with about 700 mm ef fain falling

mostly in winter, 1s condusive to the weather-

ing and |caching of the deposited ash. Stanley

(1909) analysed the basalt frona Mt Gambier

and his results are viven in Table 1. An esti-

mate of the present a¥eruge composition of

the ash, obtaied from samples A 363/T,

A 4064/1 and A 349/1, 15 also given in Table |.

TABLE 3

Relative ameuni of volcanic asic in soils

Averuge based on Average based on Dilution of Particles*

Mg, Al, Ti, Fe Cr. Man, Ni, Zn Si by ash 2-50 am Mean & 8.D-_

A363"1 100 1a0 THO 100 1b0 —

A 464/) 4 aS 53 93 S| fi

A 3449/1 &4 BB a6 93 8S 4

AASleh 66 59 a9 58 AR \4

A364/] 60 56 s7 70 61 6

A360/1 44 45 44 47 45 |

AShS/1 38 37 35 42 44 3

A 1292/1 32 25 23 32 28 §

A w58/'| 20 45 9 it 15 4

Aa67T I 14 12 a la tl 3

gg ee

* Valnes from Horton, Blackburn, & Clarke (195%),

[82 do.

For this estimate it has been assumed whut 60%

of profile A 363/17 is of Volcanic origin, 33%

of A464/l und 50% of A 349/1 and the bal-

unce is silica, and rhese assumptions sre con

sistent wilt the purticle: size distribution curve

tor profile A349 given by Hutton, Blackburn

& Clarke (1959). From comparison with this

estimated present composition of the ash ond

analysis af the basalt, ir is possible to calculate

the change in elemental composition on the

assumption that ash and basalt were from. the

sume source, The results. (Table L) show that

in the 5,000. years of exposure there has been

considerable (60-8091 loss of sodium, mag-

nesium and calcium due te the weathering of

minerals such as olivine and plagioclase uns

some Inss of potassium and iran relative to alu-

minium, silicon and titanium. The calculated

guin in these elements is due to the loss of the

olher elements and the similarity in the gutn

figure for silicon compared with those for alu-

minium and titanium confirms the assume

ratio of sand tu ash in the three soi samples.

Thus from these ratios and the data of Table 3,

ihe amount ef ash in ull ten suil samples can

be cileulared (Table +).

The relative gain of 20% in the “insoluble”

elements suggests that 20% af the ash has been

lost in 3.000 years, Le. 1% In 250 years. This

logs of 20% of the weight of ash tue to the lass

of 70% of the original sodium, magnesium and

calcium has meant considerable change hus

taken pluce. The soils with 35% to 60% ash

have exchange capacities of 30 m, equiv. per

100 @ (Clarke 1965) and in sample A 972

taken close to sample A 464 the clay mincrals

have been identified as illite, kaolin and ran-

domly interstratified material and the mixture

fas an exchange capacity of about 70 m. equiv.

per 100g (Stace et af. 1968, p, 133). Assum-

ing 12 m. equiv. of the exchange capacity ix

TABLE 4

Calewlated amroant of vacant: ask in soils

{fheafest 5%)

A 463/14 an

A 464/1 55

A 349/1 St)

ABS =n

A 3864/1 35

A 3460/1 25

A355/\ 25

A 2292/1 15

A 358/) 10

A 4a7y/1 s

HUT 1ON

due to organic matter, there is then 18 11.

equiv, per 100 g due to clay minerals, Thus the

exchange capacity suggests Lhat the cliy mitie-

rals constitute about 25% of these soils which

originally were ahout 50% ash, 50% sand, The

clay minerals have formed i sizu and have not

moved down the profile—in fact using stand-

ard Ixyboratary dispersing techniques, the soils

yielded little material tess than 2 yn. enabling

the unsorted distribution of the pariicles im the

range 2 p.m to 50 um to be used as a charac-

Leristic.

As there is no run:oit of water from the soils

around Mt Gumbier, the sodium, magnesium

and calcium released by weathering should be

levched to the groundwater, Sodium ond nap-

hesium are quite soluble and calcium is mode-

rately suluble in the presence of the high con-

<entration of carbon dioxide found in fertile

soils; As the water percolates out of the organic

soil, carbon dioxide is lost und calcium be-

comes less soluble. O'Driscoll (1960) hns pub-

lished analyses of groundwater from the Hun-

dreds of Blanche, Gambier and MacDonnell

which surround Mt Gambier. Of the samples

with less than 400 ppm dissolved solids, nine

hid beer collected either fram within the area

considered by Hutton, Bluckburn & Clarke

(1959) to have received volcanic ash or from

immediately south of the area, and five samples

oulside these two areas. The average calcium

content for each of the two awreas is 70 ppm,

while the sodium content of the walers from

the area that received volcanic ash is 45 ppm

and that oulside is 35 ppm, and for magnesium

the corresponding figures are 13 ppm and 3.5

Ppem,

It has thus been possible to confirm the

earlier map of the distribution of volcanic ash

wound Mt Gambier fMuttan, Blackburn &

Clarke 1959) und to show that considerable

chiunge has taken place in 5,000 years. About

one half of the ash has weathered to ¢lay mine-

rals with the loss of 20% ol weight und the

leached sodium and magnesium appears to

have reached the groundwater.

Acknowledgement

The author wishes to acknowledge the help

of Mr G. Blackburn, CSIRO Division of Soils.

Adelaide, Mr Blackburn collected the soil

samples and his comments on the results have

hieca valued greatly.

CHEMISTRY OF VOLCANIC ASH IN SOILS NEAR MT GAMBIER 183

References

Cuiarke, A. R. P. (1965),—A laboratory examina-

tion of soils of County Grey, S. Aust. CSIRO

Div. Soils, Div. Rpt. 7/64.

Fercusson, G. J., & RArrer, T. A. (1957).—New

Zealand 14C age measurements—3. N.Z. J.

Sei. Tech. B 38, 732-49.

Hutton, J. T., BLACKBURN, G., & CLARKE, A. R. P.

(1959) —Identification of volcanic ash in

soils near Mount Gambier, South Australia.

Trans. R. Soc, S. Aust. 82, 93-98.

NorrisH, K., & Hutton, J. T. (1964)—Prepara-

tion of samples for analysis by X-ray fluore-

scent spectrography. CSIRO Div. Soils, Div.

Rpt. 3/64.

NorrisH, K., & Hutton, J, T, (1969).—An accu-

rate X-ray spectrographic method for the ana-

lysis of a wide range of geological samples.

Geochim. et Cosmochim. Acta 33, 43-53.

O’Driscoti, E. P. D. (1960).—The hydrology of

the Murray Basin Province in South Austra-

lia. Bull. geol. Surv, S. Aust. 35 (2).

STAcE, H. C. T., Hussite, G. D., Brewer, R.,

NorrucoTe, K. H., SLEEMAN, J. R., MUL-

caHy, M. J., & HALLSwortTu, E. G. (1968).—

“A Handbook of Australian Soils.” (Rellim

Technical Publications: Adelaide.)

STANLEY, E. R. (1909).—Complete analysis of the

Mount Gambier basalt with petrographic des-

criptions. Trans. R. Soc. S. Aust. 33, 82-100.

THE SYSTEMATICS OF SOUTH AUSTRALIAN PRECAMBRIAN AND

CAMBRIAN STROMATOLITES. PART III

BY W. V. PREISS*

Summary

PREISS, W. V. (1974). -The systematics of South Australian Precambrian and Cambrian

stromatolites. Part III. Trans. R. Soc. S. Aust. 98(4), 185-208, 30 November, 1974.

Three new forms of stromatolites from South Australia (Linella munyallina, Tungussia etina, and

T. wilkatanna) are described. South Australian occurrences of Omachtenia utschurica and Linella

ukka, previously known from the USSR, are also discussed.

THE SYSTEMATICS OF SOUTH AUSTRALIAN PRECAMBRIAN AND

CAMBRIAN STROMATOLITES. PART HI

by W. Y, Preiss*

Summary

Puviss, W. V.

(1974).—The systematics of South Australian Precambrian und Cambrian

stromatolites. Part HL. Trans. R. Soe. $. dust. 98(4), 185-208, 30 November, 1974

Three new forms of stromatolites from South Australia (Linella munyalling, Tungussir

etiia, and 7. wilkatanna) are described. South Australian occurrences of Omachtenia ntxchupicn

and Linella ukka, previously known {tom the USSR, are also discussed.

Introduction

This paper is a continuation of Parts I & If

(Preiss 1972; 19734), in which the principles

of stromatolite classification were outlined and

new forms of stromatolites described. The

glossury appended to Part I also applies to this

paper

Systematics

Group LINELLA Krylov

Linella Krylov 1967: 37,

Type Form; Linella ukka Kryloy, from the

UR Suite of the Southern Urals.

Diagnosis: Bumpy, subcylindrical or tuberous,

usually walled columns with parallel to

markedly divergent branching and numerous,

often pointed, projections.

Conment; L. ukka Krylov, L. simica Krylov,

L. avis Krylov, L. munyallina Preiss, and

Ly zhuica Shenfil’ (in Khomentovskiy ez

al, 1972).

Age: Apparently only Vendian in the USSR,

but in Central Australia L. avis occurs in

rocks correlated with the Late Riphean

(Walter 1972). In South Australia, Linella

occurs in beds probably approximating to

the Late Riphean-Vendian boundary in age.

Linellu ukka Krylov 1967: 39,

FIGS. la—h, 58, 6a, 7a-e

Marverial: Six specimens from Burr Well and

Leigh Creek.

Description

Mode of Occurrence: The stromatolites form

lenticular beds, not more than 20 m long and

0.5 m thick, consisting of adjoining damed bio-

herms 2 m in diameter, In the centres of indi-

vidual bioherms, columns are vertical or

variously inclined (Fig. 7a). but ut the bioherm

margins they become uniformly reclined (Fig.

7b). Margins of adjacent bioherms ate poorly

defined. At one point, at the edge of a lenticu-

lar bed, the columns commence growth ver-

tically, but then curve over and grow horizon-

tally outwards. Biohermal beds grade into

laterally linked hemispheroidal and pseudo-

columnar stromatolites, which intertongue with

the underlying intraclastic limestone. They are

overlain by oolitic Wmestones or grey cal-

careous shales.

Calumn Shape and Arrangement: Columns ate

subeylindrical to tuberous, sometimes slightly

Nattened in various directions. Transverse sec-

tions are round. oval, rounded polygonal or

complexly lobate, 1-8 cm in diam, Columns

may swell and constrict markedly over a length

ol a few centimetres. The length of columns

between branches is usually less than 5 cm, but

individuals reach a height of up to 30 cm (Figs

la—h). Columns may he variously oriented,

from yertical and parallel to inclined at up to

45° to the vertical, but at bioherm margins

columns are radially or horizontally arranged,

Branching is frequent and varies in style from

B- to +y-parallel, or slightly divergent to

markedly divergent. Moderately divergent

branching is. the most frequent (Figs 7c.d,c).

Columns may be constricted at the base of

branching (Fig, 1a). Approximately 50% of

branching does not result in new complete

* Geological Survey. South Ausiralian Department of Mines, Box 38, Rundle Street P.O., Adelaide,

S. Anst. 5000.

136 W. ¥. PREISS

columns. bur forms marmnw, pointed, of some-

limes slightly Natlenud ougrowths | om

long. generally less than L cm in diane (Pigs

Lu-h}, These pointed outgrowths are also vari

vusly onented. and may project at a high angle

from the main column. Coalescing of adjacent

columns is Moderately frequent.

Margin Stricture: Column margins vary mainly

from smooth i gently humpy; vceasionally

sharper bumps of approximately | cm diam.

occur. Very short ribs are rarely present. Short

overhanging peaks occur in a few places, espe-

cjally near points of bridging, Bridges, where

present. consist of many laminae. A wall up to

3 mm thick is present on the whole lateral sur-

tuce not affected by peaks and bridges. The

numbet of laminae purticipating 1s dificult wo

estimate, duce ta secondary reecrystallization

(Pig, 7), Colurans ate sometimes coyted with

a selyage of fine sparry culcile, of xenotopic

equigramtiat iextute and grain size 0.01 min.

The selvage is yp to 1.5 mm thick and past-

dates the formation of the wall, but pre-dates

the filling of the interspace,

Lanitta sape varies greathy within single

columns. from almost flat or rectangular to

very steeply conyex (Big. Sa). The majority

(79% of Jaminae measured) have h/d between

0.2 and 0.6 (Fig. 6a). Laminae ate very poorly

preserved, so that their detailed shape i difli-

cult to estimate. Most are smooth, but same

are finely wavy, with 4 wavelength of 2-3 mm,

Single laminae are diflicule to follow across 4

whole column width. The degree of inheritance

of lamina shape varices along a colunin length:

in plices Jaminae chunge capidly from gently

convex ur rectangular to steeply convex.

Microsienerere ts poorly preseryed, and the

lamination is extremely indistinct. There 4s little

contrast between Jight and dark laminae,

except a slight difference in pigmentauion and

in grain size (Fig, 7d), Dark laminae are

smooth to slightly wavy sind lenticular, O,1--0.4

mm thick. Single laminne cannot be traced

right acrosé columns, partly because ol recrys~

taltivation, Upper and lower boundaries are

very diffuse and nvore or Jess parallel, In most

places, laminae are reduced to aligned lenses of

fine crained cathonatc, Dark Jaminae consist

of hypidiotopic to Xenotopie inequigranular

calcite, grain size 0.003-0.015 mm, Most erys-

tals ate lightly pigmented pale grey (possibly

an organic pigment). Id one specimen, dark

laminae are dolomilized. Subangular quartz sill

of grain size 0.02-0.05 mm occurs im places

in both dark and ligat laminae. fig! farina

ave 0,2-0,6 mm thick, and as Uiscontinuous as

ihe dark laminaé between them. They consist

either pf acicular, or equidimensional noosaic

calcire. Acivular crystals are ON-0,02 mm

wide. and are arranged perpendicular to the

laminae, and often extend also into the dark

adjacent lominae, They are therefore clearly

secondary. The equidimensional calcite is seno-

topic. grain size 0.02-0.04 mm.

Interspeces between columns are Alled mainly

with poorly bedded intraclast grainstonc. Allo-

chems, including fine pellets of dense, dalo-

mitized micrite, 0.02.1 mm in diam. and

small, flat, curved Or irregular intraclusts up to

(1.5 mm tong. are packed and mostly an contuct.

They are cemented by teunsparent sparry, xeng-

topic calcite of gmin size up tu 02 mm, A few

crude hands of dolomitized micritc, wp to |

cm thick. occur in places. ‘These are catremely

dense. fine vrained, hut contain some pellets

and intraclasts.

Secondary Alteration: Stromatolite columns

are severely recrystallized. especially near

column margins (Fig. 7d). Here laminae are

severely disrupted by lenses and irregular

patches of recrystallized, xenotopic to hypidic-

topic sparry culcile, of grain size up to 0.2 mm,

The laminge are reduced to small, inregulac or

curved, disoriented remnants; in places a see-

ondary grumous texture is developed, In addi-

tion there ate numerous irregular lenses, up dv

4 mm thick, of nearly upaque, white, fine dolo-

mite, aligned parallel to the lamination (Fig.

Fei. The dolomite is equigtunitlar, hypidio-

topic. grain size 0.01-0.02. mm. Most tntra-

clasts in the interspaces ate ulso dolomitized,

or at least surrounded by dolomitic mms, but

the spary cement is unalfected. Straight and

irregular calcite veins post-date the dolonutiza-

tion. Stylolites in places cuf across all struc-

tures of the tock, but were not seen in thin

sections. Nodules of coarsely crystalline calcite

similar ta those in /nzerlu ef. fjennsi From

Burt Well ¢Preisa 1973a) are locally present.

Compartyons

The stromatolites are identified as Linella by

their bumpy, subcylindrical and twberaus,

parallel to markedly divergent branching.

walled columns, and numerous pointed pro-

jections. Many specimens of Baicelia have simi-

lay gross shape, but lack the almost ubiquitous

wall and the numerous pointed projections of

Linella. They are usagned 1) Linell nkka

Krylov on the basis of cohimn shape. style of

SOUTH AUSTRALIAN STROMATOLITES If

branching, and) margin struciure, Linlike L.

Mfrved Krylov, ribs are poorly developed or

ubsent. The columns are more broadly bumpy.

more divergently branching. und Jess enaried

than those of 4. avie Krylov, Micrastracture is

less well preserved than in the type material

but lamina shape is very similar. Linetla uhkba

from Burr Well is very similar in microstruc-

lure, Margin aructure, lamina shape and mode

of preservation to Gynmmasele cf ranivayt

from limestone clasts in the Tapley Hill Fm.

but is distinguished by its bunmpier, more tuber-

ous, divergently branching columns Krylav

(1967) deserihed Thgussid bavse as a separate

form, but states that it veeurs at the margins

of Linella ukka bioherms. Similarly. at Burr

Well, inclined und horizontal columns occur at

biohenm margins, bul these are here included in

Finella ukke. L. zheicea Shenfil’ rarely has a

wall,

Disitibution: Uk Suite of the Southern Urals

and in beds correlated with the Kiyktan

Suite of the Central Urals. USSR: Balca-

noona Formation, Burr Well ang Leigh

Creek, Northern Flinders Ranges, S$, Aust,

Linella aff. DC. ukka (Cloud & Semikhatov

(969) occurs in the Johnnie Formation,

South Ibex Hills. California, USA.

Age: late Adeloidean: in the USSR it is

apparently restricted to the Vendian.

Linella munyatlina f. nav

FIGS, li-y, 2a—n. Sb, 6b, 8a—t, Jn-c

Materlel: Twenty-six specimens frany West

Muunt Hut. Termination Hill, Lake Arthur.

Myctle Springs, Burr Well, Roebuck Bore

and Arkaroola “reas.

Helory ov: S495 (Figs. 1x.y. 2a cs 9b), S km

east of Myrtle Springs.

Name: After Munyallina Valley, where the

stromatolites of the Arkaroola srea oecur.

Diagnosis; Linella with vommantly parallel

branching, a wall chat is discontinuous on some

columns, and with highly variable lamina

shape. Columns ute gently bumpy. and pointed

propections are subordinate.

Description

Mode of Occurrence: ‘Vhese stramatolites afc

widespresd in the Wundowie Limestone of the

Northern Flinders Runges, where they occur

in dented biostromes and lenticular heds con-

sisting of contiguous domed hicherms. com-

monly overlain by thin sandy limestones, and/

or interbedded in green of red shales. The biv-

stromes vary in thickness in different areas

187

from 450 cm to 2 m, depending on the reef of

the Individual bigherms they comprise. At Burr

Well. individual bioherms ate isolated (Figs.

Sa.c.d) of cantizuous, so that stromatolite beds

are Jewticular, and recur at different strati-

graphic levels. These bivherms, with growth

relief of about | m, are of ellipseidal shape,

with strongly inclined columns at their margins.

Luminated shale or liniestone fills the spaces

between bioher'ms (Figs, 8a-cl; in places, sandy

limestone Taps on to the bicherm margins, and

then covers the whole biostrome or bed, Trans-

verse sections of biofierms gre rarely seen.

except where dips ace gentle: e.g. neur Myrtle

Springs oval bioherms occur, while at Arka-

roola they are sintious and irregular. Sill. iso-

lated bioherms only 30 em wide also occur at

Arkaroala,

Colunin Shape and Arrangement, There 1s

great vurtability of column shape even within

single specimens. Most commonly, columns are

vertical or inclined, gently curved, non-parallel

and bumpy, varying from subeylindrical to

tuberous (Figs li-y; 2a--is Ref 99<)-

Columns vary in diam, from | tu 8 cm, and

swell and constrict moderately throughout their

length. Transverse sections are conimanly eval,

vatiously elongated. lobale ar rounded-polv-

gonal, occasionally circular. Columns are up

to 10 em long hetween branches, but indivi

duals utlain 4 height of ubout SO cm, The ter-

minations of colunins may be either rounded

or pointed (Fig lprtx.y). Columns are

poorly developed in the bioherms at Arkuroola,

where they are bridged over after a few centi-

inctres Of growth (Fig. AF

Sranching ts yery frequent. variable, but most

commonly subparajlel (mostly a- and (-

parallel, some y-parallel) and moderately di-

vergent, (Figs li-y; 2a—m: 9a-c). In all speci-

mens, there are a few branches which do not

erow inte Jarge columns, but terminate as nar-

ruw, pointed projections, 14+ cm long, after

jess than 1 om wide (e.g. Fig. 1x,v)_ These pre

subordinate and muy either be parallel to the

main culumn, or diverge from it laterally.

Margie Structure; Columns are moderately

bumpy: in general the bumps are low, rounded,

1-3 cm in diate. and with a relief of usually

less than 0.5 cm, Bumps may grade into short

pointed projections. Some cohimns from

Myrtle Springs are tather smooth (Pigs lw).

The margins of colunins are mostly Walled, But

fur short distances the wall may be obsent,

Short overhangilig laminae and peaks are pre-

SOUTH AUSTRALIAN STROMATGLITES fil

sent moderately frequently, white adjacent

columns are sometimes Linked by bridges of

varyme thickness. Same inclined columns at

biohuras margins at Burr Well are largely

unwalled (Fig, &e), [i many oulerops. cohinns

afe scen te he bovged over at the top. The wall

is formed by che marginal portions of both

stecply and gently convex laminae covering the

lave surface of colunins, bul ihe number ot

Taniinac participating is dificult to estimate,

ilue to recrystallization of the wall vone. Well

prescrved specimens from Myrtle Springs show

that up ty 20 daminace may he involved, the

wall zone here hemg up ta 5 mm thick (Fig.

Yh),

Lumina shetpe is highly variable (Fig. Sb), with

a large spread of values of h/d from 0.2 to 1.3:

the greatest variability is seen in single speci-

mens ut Myrtle Springs, and lyminse fron

other areas fall within this range: 764% of lami-

nae measured have h’d between 0.3 and 0.7

(Fig, ob}. The mnst steeply convex laminae

occur in the pointes) columns at Myrtle Springs,

where they approach subconical shape; other-

wise laminae are smoothly dumed. rarely rect-

angular or flattened. On a finer scale, well-pre-

served laminae are smooth or very cently wavy!

no primary wrinkling is seen, although in some

specimens, recrystallization has embayed

laminve so as ta produce w secondary wrink-

ling.

Micrastriieiure is best preserved in specimens

from Myrtle Springs, where it is seen to consist

of thin, even, jight and dark laminae, which

are generally continuous, but may be cut by

small micro-tinconformities, Bath lamina types

thitt markedly and become more dislinct to-

wards the column margins. Laminac are espe-

cially prominent in the wall zonc, where they

are of more uniform thickness (0.05-G,L mm),

with smooth, parallel boundaries, but lens aut

gradually down the column margin (Fig. 9b).

Here dark laminae, composed of an interlock-

ing mosaic Of Acnolopic calcite, of grain size

0.008412 mm, alternate with lighter laminae

of similar texture and slightly coarser grain size

(0.0135-104 mm), In the central portions of

coluntins. laminae arc 1 to 0.5 mm thick, the

pale laminue generally being thicker than the

Fig. 1.

189

dark. The laminae wre of similar texture and

gin Size 16 those at coluiin Abarains, hut the

lizht laiinae contain ahundanr irregular, xeno-

lopic dolomite crystals of grain sive 0-03-0.05

rum, Microstructures. From other sreas are less

well preserved: frequently the finest laminae

have been obliterated by greater dolomitizalion

fe.g- Roebuck Bore, Fig. 9a}, of by more per-

vasive rcerystallization of (he limestone. Small

areas with unaltered yery thin laminae usually

occur as remnants of the anginal microstruc-

lure,

Interspaces: The sediment filling jaterspaces

varies from urea to urea. At Myrtle Springs,

columns ure widely sepatated (1! to 10 em

apaTt) and the interspace sediment ws Inyered,

vonsisting of Hiternuling bands pf sand and

micritie limettone. The imicritie bands are

homogeneous, 2-25 mm thick, aod consist of

slightly recrystallized Xenotopic calcite (rain

size 0.003—-0,01 mm) with rare: scattered doto-

mite rhombs. In places; algal laminae form

continuous bridges capping the iops of

columas, but alsa oceur as upward-concave

laminated sediment between walled columms.

indicating “that they post-dite the column

erowth, Such algol laminae may in tum grade

up into new columns. Both the miecrite and the

algal laminae are scoured in places to a depth

of up to 3 em, and the channels so formed are

filled with coarse sand, of grain size (} 5-2 mm,

with ooids, minor lime mud, and cemented by

fing, sparry and acicular calcite. The growth

relief of columns must have ¢xceeded abour

5 cm above the surrounding sediment, which

was formed hy slow deposition of time nud

und periodic rapid deposition of coarse detritus:

Intraclastic limestones (alten sundy), oecur at

Rocbuck Bore (here intraclysts gre Hinestone

While their matrix is dolomitized} and Birr

Well (Figs. 9a; 8), Intraclasts are randomly

oriented, slightly wwounded, \strictureless flat

pebbles up to { cm lopg, consisting, of recrys-

tallized xenotopic culcile of grain size 0.0}—

1,03 mm. The matrix consists.of equigranular,

Rcnotopic dolomite of grain size 0.05-0.03 mm

with minor fine..quariz Sand ang iyon-stained

dolomitic peltets.Specimens frany the mickile

member of the Wundbwie Liviestane at Arka-

=i ‘

Reconstructions of Linella, Umberatana Group Bundess: Rangers; acta) Linel i akka, Bal-

canoona Formation, Burr Well; (a, b, 1, -hJ—S478:. te, S477 oy |

(d)+-$541, (i-qi—

Linella muasatiing. Wundowie Limestone, Member, Rogbuck, Bore: (j, ke hin, 1) --S43 1) (9)

—S430; (i, @}—S428: (m)—S427; (rv) ~ tincHa marvalling, Wondowie-Limestone Mem-

ber, Burt Wells (1, t, ¥)—S486; (s, W—S8484, Inchned columns. from bioherm margins; (w,

x. ¥)—bLinella muityalliia, Windowie Limesjonc: Member, §-km east of Myrtle Springa 4.5,

Holotype $495.

78h

rola contain handed interspace sediment; the

alternating bands. up to J cm thick, coitain

micrite and fine intrusparite respectively, sug-

gesting periodic current action to rework Tie

mud fragnicnts, In [he upper member of the

Wundowie Limestone at Atiarac”a, interspaces

ure filled with homogeneuvus fine subangular

quartz sand, cemented by minor calcite

Sceondary Alteration: Specimens trom Myrtle

Springs are best preserved, the chief alteration

being partial dolomiuzation of light laminac.

Altecation of the wall zone by recrystalhzatiun

of calcite is common in all wraas: the outer por-

tions of laminne are recrystallized to an equi-

vranilar, hypidiotopie calcite mosaic. Where

recryslallization. is slight, a few relics al dark

Inminae ure preserved in a sputry calcite

mosaic, Of grain size 0.03 40.05 mm. often with

scattered dolomite crystals, With extreme re-

crystallization, the whele of « column may be

alfected, resulling in a coarse hypiciotopic

mosaic of cquidtmensianal, twinned calcite

crystals, (5-2 mm diam, A secondary green

clayey mineral forms an interstitial matrix be-

tween calvite crystals. and probably represents

u segregation of impurities during recrystalliza-

tion, Even in these cases, the wall is usually

preserved as a thin layer of very fine calcite,

and the interspace outside it ts unaffected.

These patches of coarse teerystullization, to-

ecther with the fine calcite veins they grate

ino. Apparcatly post-date the dolomitization of

light laminae, since relics of this dolomite ure

preserved within them, Specitnens from Ree-

buck Bore are very largely dolomitized, appre-

ciable amounts of culcite being preserved only

in the columns and in some intraciasts_ ‘The

imterspace matrix is completely dolomitized.

dolomitization predating styloliies. and calcite

veins.

Comparisons

The stromatulites from the Wundawie Linte-

stone at Myvtle Springs, Burr Well. Rocbuck

Rore sud the Willouran Ranges are identified

Fig. 2.

W. Y~ PRESS

as TLinella on the basis of theit branching.

bumpy, tubcrous columns and ihe presence of

a wall and pojnied projections, Specimens from

Arkaroola are also included, although here the

columnar keds ure thin. and columns rapidly

cualesce or arc bridged over by wavy-laminated

stromatolit ~ nella munyallind is similar to

Kalyaria + rensis Preiss and KRulavia ves-

rota Preiss in having bumpy walled columns

‘Acti pointed projections, but the columns of

the lalier two forms are more closely spaced,

subcylindrical and always parallel, with no

divergent branching. Lonel munyalling is dis-

tinguished from Lb, whka Krylow by its demi-

nantly parallel branching. fewer pojnted pro-

jections, the presence of moderalely frequent

peaks, brides and unwalled patches. of

columns. Lirella simica Krylov has ribbed

columns, while £. awvis Krylov tas more

gnarled, thickly walled columns with very fre-

quent pointed prujections. L. z/atca Shenfil’

rarely has a Wall and has markedly divergent

branching.

Distribution; Widesnread in the Wundewic

Limestone, Umberitann Group. of the

Northern Flinders Ranges: neuer the West

Mount Copper Mine, 5 km east of West

Mount Hut. 9 km north af Termination Hill

and at sake Arthur, Willonran Ranges;

middle member of the Wundowie Limestone.

8 km cast of Myrtle Springs; lower member

of the Wundowie Limestone. Burr Well:

middie member of the Wundowie Limestone,

Roehuck Bore; and Jower and upoer mem-

bers of the Wundowie Limestone, 2 km

south of the Arkaroolw Airsirin. A small

specimen from the South Australian

Museum collection (supplied hy Mr. N.

Pledge), found in the Btina Formation near

Arlipena Hut. Central Flinders Ranges, east

of Martin's Well nay alsa be Linella niun-

yallina.

Age: Late Adelatdesi, correlated with cither

the Late Ripaean o"' Vendian of yhe USSS.

Reconstructions of Linella miunyeilina, Qmachtenia wtachutica and Pangussar etina, (a-%)—

Livietle muotyallina, Wandowie Limestone Member; (a, b, ¢)- Holotype $495, 8 km eust ol

Myrtle Springs H.S.,

fd. 13 —S549, Lake Arthur, south-western Willouran Ranges (Collected

by Mr, B. Mucretl); fe)—S485. Burr Well; (F)-

£556, West Mount Hur, Willouran Ranges

(Collected by Mr, Bo Murrell); (g, h)--S48A, Arce Well; (i)—S552, Lake Arthur, South-

western Willouran Ranges (Collected by Mr. B. Murrell); (k1—-S'44, 3 km east of Copley;(L)

—S555, West Mount ..ut, Willourag Ran

3 (Ce) cled by Mr, B. ofurrelll, (m)- $366. 9

km north of Termination Hill (Collected by Me. B. Murrell); ia) —S284, Menyallina Vil-

ley;

Neput Creek} (o, p, T)—S39S> ty)

eras; (s)—SIS8, Turiguasia etina,

(o-F)—Onachenia wfschuriea, from the uppermost beds of the Tapley Hill Formation,

-$392_ Note; Not all bridges could Se shown on dia-

Flinu Foumation, & km east of Blingtaby (t)—SIS7,

Tareussia ena, Etina Pormutlon, Enorama Creek.

SOUTH AUSTRALIAN STROMATOLITES III 19]

SA Dyeareiiene of Phe

Growp OMACHTENJA Nuzhnoy

Collena omachiensis Nuzhnow '96eQ: 1422.

Omachtenia Nuchnav '967> 134.

Type Por: Omuclvenia anvichtersis Nuzhi-

ney, from the Omakhtin Suite of che Uchur

Busin, Uchuro-Maya region, S.E, Siberian

Plstform.

Pjagnesivs Columnat-layered stromatolites com-

sisting of cylindrical and subeylindrical un-

walled columms, frequently widening \pwards,

wilh mumerous cornices and bridges linking

several columns. Rranching is mainly w-parallel;

colunins are usually vertical, sometimes cadiat-

ing or curved,

Cantent: Omuchrenie omachreasis Nushnoy,

O, weechurieg Nushnov sad O. givimnensty

Nuzhoy.

Age and Distribution: Early Riphean in the

Uchuro-Mayy region of the USSR, but Jn

South Austrulix, QO. wtschuriea occurs in

rocks correlated with the Lite Riphesn,

Ontachtenia utschurices Nuizhnov 1967. 133.

TIGS, Jo-r, Se, 6¢, Fle, 10a-c

Material: Nine specimens trom Depot Creck

and Mundallo Creek.

Description

Made ef Occurrence: The stromatolites form

small lenticular bioherms repeatedly inler

culated jn very finely laminated calcareous silt-

stones of the top of the Tapley Hill Formation,

south-western Flinders Ranges. Commonly dis-

erele, biohermis 2 ta several tens of metres

wide, develop on ¢rosionyl surfaces on the

underlying laminated siltstones (Preiss 1973h,

pl. 28) and are closely assucisted with chan-

nels Aled with imbricuted flat-pebble breccias,

often surrounding the bioherm. Bioherms are

generally less than | m thick. All gradations

from flat-laminated to domed, club-shaped,

psudocolumnar and columnar stromatolites

exist (Figs. 20-7, 9d.c), Where columis are

developed, their axes are mostly vertical, but

their sides may slope in various directions, and

overhang the interspaces (Fig. 10a).

Calum Shape and Arrangement: Where

columns are discrete, they are generally sub-

cylindrical. sometimes widening upwards, either

vertical, or radially arranged. Columns are

rarely completely discrete for more thin w tew

centimetres, but are either linked by bridges or

coinpletely coalesced. They may pass htlerilly

as well as vertically inio laterally linked or flat-

laminated stromatolites, which miiy in turn pass

mio fiat-pebhle breecia, at feas| some of the

intraclasts being rewnrked chips ef algal mats

W. V. EP REISS

Columns commonly commence growth upon

some irregulanty of the subsiratum, e.g, on the

erosional surface GF the underlying sills or on

upturned flat pebbles (Fig, 2p). Calumns ire

mastly circular in cross section, 2-15 emi in

diam., but may be eomplexly lobules

Branching; True branching into discrew

columns is moderately rare, but may be mul-

tiple. Branching, may he n- f- Or y-parallel,

sometimes markedly »-parallel. or slightly di-

vergent. Branched columns ure frequemly

bridged over, of coulesec, after a few centi-

metres.

Margin Sirvcture: Column margins are

exteemely inregular with numerous short cor-

nites, bridges und overhanging laminae, which

drape over the penodically deposited interspace

ecdiment (Fig. 10b). Bridges consist of from

one to many laminae, up to several centimetres

thick. Over intervals withouw! bridges or over-

hanging laminae (whicl may represent periods

of growth during which interspaces were not

filled) the column murgin bears small ribs and

bumps. Nowhere is a wall developed.

Laming Shape: Larninac are never steeply con-

yext i most cases, they are Mul-topped, with

Jown-turned edges, 1.2. rhombic or rectangular.

They may grade both laterally and vertically

into continuous Alal fominac, Typical lamina

shapes ire illustrated in Fig, Sc, Of 40) Jaminue

measured, 83% have h/d belween 6.2 and 0.4

(Tig, fc), W the growth of a column ts isym-

metrical, lamjnae are plso asymmetrical, but

growth always proceeds vertically. although

column sides may he sinping, Laminate are

smooth, very rately wrinkled or finely wavy,

occasionally with micro-unconformilies.

Aficrostructure is distinctly banded and con-

sists of an alternation of sparry and pelletal cal-

cite Jaminae and fine. granular dolomite

laminae (Fig. 10b,c). Dolomite laminae are

0.2 to 1,0 mm thick, and chin only slightly

lowards columo margins. Their upper and

lower boundaries wfe more or less parallel; the

upper boundary is always shurp and often

smooth, while the lower Js usually gradationsl

into pelletal laminae, Delomite laminac. with

almost no calcite, consist of granular, equi-

dimetisional hypidiotopic to idintopic dolomite,

grain size 0,01-0.03 mm. At the boundaries,

euhedral dolomite crystals protrude into the

adjacent sparry laminae. In places, several thin

dolomite laminae are grouped to form macro-

laminay up lo 2 mit thick, bere (he dolomite

laminae are separated by thin, discontinuous

SOUTH AUSTRALIAN STROMATOLITES IL

lenses of sparcy calcite. which may be open

space fillings (Fig. 10b),

Dolomite layers are everlain with sharp and

sometimes Sighily eroded contact by coursely

spatry calcite lamihyt xurying in thickness

from O.1-14) mm, which pinch and swell sud

may lens out laterally. The calcite 3s hypidia-

topic tO xXenolopic. transparent. consisting of

frequently twinned crystals, grain size O.04—

0.2 mm, Tn places there are lenses of coarser,

polygonal calcite of gruin size up to 0.6 mm,

und tTarely, ot acicular caltite. Scattered very

small dolomite rhombs occur in places, Sparry

calcite laminae grade up into pelletal laminae,

consisting of subrounded pellets 006—-0.1 mm

in diam., of fine grained hypidiotopic dolomite

(0.13-0,02 mm grain size), with clear, xeno-

lopic calcite cement filling the yoids. Pellets

become more tightly pucked upwards, so that

they grade into homogeneous dolomite laminae.

In one specimen (Fig. 1fe) pelletal Iaminac

ure poorly developed,

Interspaces between columns are Aled with

intraclast and pellet grainstones. periodically

interrupted by hricging Inminae, Essentially the

Sime sediment occurs outside the bioherms in

channels cut into the underlying silts, but there

it is bedded, and clasts are imbricated. In the

interspaces, the sediment is largely unbedded

(Fig. 10a,b) consisting of flat intraclasts wp to

several centimetres long, I-} mm thick, ran

domly oriented and loosely packed with numer-

ous Tound to ovoid pellets, 0.15-0.3 mm im

diam. Peliets and intractasts consist of equi-

granular hypidiolopic dofomite similar to that

of the dolomite Jaminae; the fntraclasts were

prohably derived rom the erasion of the flaut-

laminated varicty of the sifomatolites, while

pellets are interpreled as comminuled and

rounded, repeatedly reworked dolomite intra-

clasts. Allochems must have been in part matrix

supported, but oily locally is a Time mud mat-

TIX preserved. Must grains are cemented hy a

clear, sparry cement of xenolopic inequigsranu-

tar calcite, grain size up to 0.4 mm. Whar must

have been primary lime mod supporting scat-

tered intachasts now censisty of recrystallized

hypidiotopic calcite. grain size 0,05-0.1 mm

with scattered dulomite rhombs. In places, large

allochems or overhahging column margins shel-

tered the underlying areas from settling mud,

and these are now filled with course, open space

filling sparry calcite,

Secondary Alteration; Dolomite pellets and

intraclasts were probably sewerked as dolomite,

193

i.e. the oviginal sediment was affecteil by early

diagenctic dolomitization and then redeposited:

maoy intraclasts are long and flat, and could

not hove withstood transport without being

lithified. ‘I hese allochems were partly supported

by lime mud. and partly winnowed, leaving

open spaces filled! wiih sparry cement. The time

uf dolomitization of the dolomitic siromatolite

laminae is nol clear; dolomite pellets are

cemented with spurry ealette, suguesting that

the sediment was brought in as dolumite. But

dolomite rhombs in the laminac appear to pinst-

date the culcite cement. Ln aduitten, dolomite

rhombs occur seuttered throughout the reerys-

tallized lime mud (now mictospar}, and the

Sparry, open space filling calcite. It is likely

that minor secondary dolomitization affected

the whole sediment after its deposition. Post-

depositional pyrite cubes, 0.08-0,20 mm wide,

are scattered throughout the rock. Stylolites are

fare, wnel ame restricted to hroad|y conformable

\ypes which follow bridging laminse between

Columns.

Camparisens

The columnar and colurmnar-layered portions

uf this stramatolite accord with Nuzhnov's des-

cription of Guyachtenia in having eviindsical or

sub-cylindrical columns with frequent cornices

und overhangs on the lateral surfaces. which

are linked by numerous bridges and Javers

commer to several columns. Branching in bok

is dichotomous or multiple, usually o-parallel.

Columns are usually vertical, or rarely, radiat-

ing. As the domed and flatlarnimated. sirama-

tolites cannot be separated fram the columnar

and columnar-layered portions. these must be

included ous environmental variatlons of

Omachtenia, The stromatolites differ from

Jurusania Krylov and Kussiella Krylov in hav-

ing more wregolar, more Frequently branching

columns repeatedly linked by bridges. The

repeated bridging and characteristic thick. pel-

letal luininae distinguishes them from the basal

portions of Inzeria conjunete and Acaciella

ages. OC. utsehurtca Nuzhnov differs from

O. aivunensis Nuzhnov in having more gently

conver laminae (h/d less than 0.5). GO. etach-

teasis Nuzhnovy has genenlly narrower columns

and some short, lateral outgrowths. und thin-

ner, non-pelletal laminae. O. urschurica from

the Tapley Hill Formation is extremely similar

it gross shape, tvpe of bridges and lamina

shape, but has slightly thicker pelletal Jamnae-

(Pellets may also be present in the type muite-

194

rial, as in Nuzhnov 1947, Pl. 11¢4)). Omtach-

tenia closely resembles Schuncheria Korolyuk

in pross shape. lamination and bridging; Schan-

elaria, however, appatentiv has a thin, one-

layered wall (Korolyuk, 1960),

Diseibetion; The Omakhtin Suite of the

Orhur River, 8-E, Siberian Platform, and the

upper Tapley Hill Formation, Depot Creek

and Mundallic Cresh, S.W. Plinders Ranges,

S. Aust.

Age Early Riphewn in the USSR, but here iL

is Late Adelaidean, in beds correlated by

other stromatelites with the Late Riphean,

Group TUNGUSSIA Semikhatov

Collecie suvkerwigusica Semikhatoy 1960;

1481.

Tungussia Semikhatoy 1962; 208-

Type Form: Tungassia tedoso Semikbotov,

from the Sukhotungusin Suite. Yunisei

Mountains.

Didgpesiv: Tuherotis to subeylindrical, heri-

zontal to vertical columns with frequem, mul-

tipfe, markedly divergent branching; lateral sur

face is smooth or with small peaks, and at least

locally with a wall.

Corient: T. Hodosa Semikhatov, T. conftase

Semikhatov, T, sibiriee Nuzhnoy, T. inet

Walter and 7. ereern Walter. T. bassa is a

lateral variant of Linella ukka Krylov, 7.

enpiggent Ruaben and 7. rvsva Raaben are

itwulliciertly described and illustrated to

allow comparison, and the description of 7.

weties Raaben is unavailable. New forms

are T. eine and T, wilketenaa.

Aye: Middle to Late Riphean. and probably

Vendian,

Tungussia ¢tina {. oy.

FIGS, 25,0. 3a—-m, dab, Sd, 6d, Ode, J 1a-«,

l2a

Materia!: Twenty-eight specimens lrom Mt

Chambers Gorge, Teatree 0.8... Blinman,

Martin's Well, Enorama and Arkaba areus.

Holorype: S435 (Figs, 3i,1, dab, 1c), Me

Chambers Garge.

Nanw: After the Etina Formation, in which

the stromatolites partly occur,

W. V. PREISS

Diagnosis; Tungussia with a wide varlation of

branching style from subparallel to markedly

divergent, a thin, interrupted wall, and thick,

pinching and swelling, wavy laminue. Coarse

detritus can be incorporated in Jight laminae,

if it Was available during growth.

Deyeription

Mode of Occurrence: The stromatolites occur

in irregular tonguing bioherms and lenticular

beds in the Elina Formution and ils extensions

in the Northern Flinders Ranges, Exposures are

often inadequate to determine the cxuct shape

of the Jenyes, but generally they are discrete

welated bodies, surrounded by sandy and

oolitic limestones. Tn the vccurrence neur Mt

Chambers Gorge, the columnar stromatnlites

overlic irregulatly laminated sandy and oolitic

limestone (the contact is now stylohitic), and

form a lens up te 2m thick in its thickest part

In places, growth continued on the 3p of the

lens in the form crt inegularly wavy and

pseudocolininar stromatolites. At the margins

of the bioherm, columns grade laterally into

psenduco!umns and Wavy Jaminac, which inter-

tongue with oolitic limestone. At Teatree O.S.,

the stromutolitic bed again intertongues with

oolitic limestones, but hete columas are mere

inclined at toe hioherm margins than tn their

centres. Siniar relations of slromatolitic bie-

herms intertonguing with sandy oo and intra-

clast grainstones were observed in the Elina

Formation in the Arkaba Hills, Enorama Creek

(Fig. 10c), Blinman and en the south-western

fiank of the Enoramu Dispir. However, at

many locations in the Central Flinders Ranges.

the colurnnar portions are poorly developed.

Calumnar Shape and Arrangement: Well deve-

loped columns persist vertically for more than

10 em only in the sections ar Mt Chanbers

Gorge, Enorama Diapir and at Teutree O.S,;

elsewhere short, irregular columns quickly

prude up info linked pseudocolumns, At Mc

Chambers Gorge, the orientation of columns

varies [rom vertical to variously inclined, to

subhorizontal (Fig. 1d), Columms from the

Teatree GS, locality are also variously inclined,

but rarely subhorizontal; some are subparallel

(Figs 2s.t. 12a), Columns from all areas are

tuberous, bumpy. swelling and constricting. or,

nig ANA

Fiz. 3.

S km east of Blinman;

Revonstractions of Trngwrsie etina, Umberatane Group, Central and Northern Flinders

Ranges. (a|—S286, Wundow Limestone, near Teatree O.8.;

{(b)—S148. Etina Formation,

(e)—S56L, Etina Formation, S.A. margin of Enorama Diapir: (d)- -

§522, Buna Formation, Arkaba Hills; (¢) —S526, Balcanoona Formation. near Mount Cham-

bers; (f. g, I)—Wundowie Limestone Member, near Teatree OS; (£) S441, [z) S444, (h}

$440: (i. 7, k, mJ—Balcanoona Formajion, nen Mount Chambers: (i, $}—Holotype, $433,

(7) —S436, (kj—S525. (m)—S524,

SOUTH AUSTRALIAN STROMATOLITES IIL 19

(San dee Fiz. 3. SA Dap tid oh tates

196 wiv

less commonly, straight, subcylindnical Short

columns from Central Flinders locylities are

Frequently bulbous (Fig. did). Bumps and

swellings are generally bread and rounded,

while constrictions sometimes tuke the fornt of

dcop indentations into the main colunin, at

poms of branching (Fig, 3a,ih). Some

columns branching from the main column ate

only u few centimetres long. with either pointed

or TOwnded terminations (Fig, 3a). Columns

vary greally in diameter from | to 10 cm, the

largest oceurning at Mr Chambers Gorge.

Transverse sections vary irom ellipucal to cam-

plexly Jubate: circular sections pre rare.

Branching is yery Frequent and highly variable;

even within single specimens, both parallel and

markedly divergent branching may occur. Spe-

cimens from Mi Chumbers Gorge have prt

dominantly multiple, markedly divergent

brimehing. although columns may became sub-

pacallel soon alter branching (Fig. 3m). At

Teutree O.S.. otrkedly divergent branching

and purallel or slightly divergent branofring

pecur together (Figs. 3h, Ila, L2e)

Columus from Enoranm Creek are frequently

rnincated hy siyluliies paralicl to tverall bed-

ding, so that the style of branching is ahscured.

Columns fram this locality that allowed recan-

struction (Fig. 2L). show markedly divergent

branching,

Margin Siruesiees Primary margin structure is

frequently obscured by stylolites; in some speci-

mens from Arkaba. Teatree O.S. and Mt

Chambers Gorge, alnest no column margins

ure preserved. Where columns are. relatively

unallected by stnlites, they are seen to bear

thin, antcrrupred walls. involving two or three

laminae only, or very locally, multitaminate

walls, cg. Enorama Creek and Teutree OS.

(Figs. |la,hy}, But Whe latler ave affected by

pervasive reerystallization, sa that commonly

only the outer murgin of the wall is preserved.

Adjacent colurins frequently coulgsee, Or are

inked hy mussive bridges up to several centi-

metecs thick. Bridges and overhanging laminae

ure common on unwalled porions of columns.

especially {roms Mt Chambers Garge (Fig,

3m). Column margins are gently bumpy, with

gecasional short transverse ribs Must of the

surface irregularity of some specimens finn

Teatree O.S. ig due to stylolitic solution of

column margins (e.g. Fig, 3a)-

Lamina Shape is most commonly moderately

stveply convex (Fig, 5d). Measurement of h/d

rauio is difficult in same specimens de to

removal of column margins by stwlolitte solu-

PREISS

tions thus measured ratios nay be tog low ih

Ihese cases, OF 131 Jaminue measured, 93%

have ratios of h/d between (2 and 0.7. the

mode being between 0.3 and 04. Laminae are

moderately to thurkedly wavy, the undulations

having a wavelength of 3-10 mm, and aypli-

tude 1-3 mm. Laminae are lenticular. ani

pinch and swell murkedly over short distanves:

this irregulacity if caused at least in part by

erosional micrn-uncanformities (Fig. [1ce}.

Micrayructrrsy A broad, irregular lamination

is well pfeserved in some specimens [rom Tea-

tree O.S., Blinman, Enoruma Creek and Mt

Chambers Gorge. where thick, wavy, pinching,

and swelling light laminae alternate with darker

thin, fine-grained laminae frequently with clay

or iran oxide impurities, Ligh! lanunae vary

rapidly in ubickness from 0.2-2.00 mm, and

frequently lens out laterally; few exten geross

a full colunin width. Very commonly, the Jight

laininac are truncated hy erosion sttrlaces, espe.

cially in specimens from Mt Chambers Gorge

(Fig. tte). They are composed al equigranotar

Xenotopic ta hypidiotepic mosuic caleile, grain

size 0.006-G.03 mm. Gccasionally, coarser

detritus is incorporated. if it was available, For

¢xample, the Enorama Creek stramatolites con-

tain up lo SUS: of ooids and coated grains,

0.3-1.00 mm in diam., within their light lami

nae. Elongated ooids aml coated prains are

aligned parallel ra the lamination, and are

always supported by the finer sediment of the

stremuatolitic Jaminae, Ooids are extremely

abundant in the inlerspaces. Specimens from

Teatvee O.S. contain very few ooids, but here

the supply was not great, as seen from the pre-

ponderance of linve mud in the interspaces, At

Mt Chambers Gorge, ooids are absent both in

interspaces and stromutolite Jaminse, but fine

sand present in inlerspices ix also incorporated

into Jaminae. These observations suggest that

the algal mats were cupable of trapping coarser

detritus, if it was brought to the sile. The

thinner dar& laminae ate 0.05-0.15 mm thick,

and composed of very fine micritic calcite, of

xenotopic, equigranular texture and prain size

0,002-0,01 mim. At Mt Chambers, the dark

laminae ore emphasized by very fine, hypidio-

uipic ferruginous dolomite cancentrated along

them. In places (e.g, Blinman!, dark laminae

with shatp lower boundaries grade up mio lizhi

laminae (Fig, 11d), At Arkaba Hills, the dark

laminae are largely stvlolitic.

lnterypaces: Columns are moderately closely

spaced, interspaces 5 mm=2 em wide, The type

SOUTH AUSTRALIAN STROMALOLITES UT 197

of sediment fillicgg the interspaces varies in the

Uifferont prods, and its relation to the quantity

of detritus in laminae has already been dis-

cussed, At Mr Chambers Gotpe, interspaces

are filled mainly with slightly dolomitized and

recrystallized puctly laminated lime mud. with

a few bands up to 2 cm thick of very fine, sub-

angular yuartz sand. Flat intraclasts up ta 2

cm long are in places stacked vertically in inter-

spaces hetween walled columns. indicating a

minimum relief of 2 ¢m_ Discrete areas af

intraclast grainslone suggest that ufter column

erowth, coarser detritus was occasionully

washed in hetween times of settling of lime

mud. At Teatree O,S. interspaces contain

poorly bedded micritie limestone and ooid

wackestune: in one specimen (Fig. 11b), these

alternate in 5 mm bands. Ooids are commonly

preserved only as moulds infilled with sparry

culcite. Unbedded fine or medium sand with

micrite matrix commonly fills interspaces. in the

Etina Formation, At Blinman, the sand con-

tains rounded medium grained quartz, red

feldspar and green pellets consisting of a chio-

titic mincral. Since little sand is incorporated

into the stromiitolitic laminae, the interspuces

were probably rapidly filled after. not during.

column growth, Interspaces at Enorama Creek

are filled with ovid grainstone exclusively—the

ullochenis are chiefly ooids with a sitgle outer

Jamina and coated, flat intraclasts. Oolitic

jaminug may be partly detached, perhaps due

to the growth ol sparry cement,

Secondary Alteration: Specimens from Blin-

mun und Enorama Creck are the best pre-

served. the chief alteration being the formation

of cyicile veins, cut by liter stylolites parallel

to bedding. Doloniitization is restricted to spe-

cimeny from Teatree O.S. anc Me Chambers

Gorge: rhombs of dolomite varvilig fromm 0.01~

0.015 mm, sometimes ferfuginnus, are scat-

tered throughout both lamina types. Ferru-

gmuus dolomite is concentrated in the dark

laminae and the interspace sediment at Mt

Chambers Gorge. Small areas of reerystatliza-

tion of fine srained calcite to grumous texture

are present in ull specimens: the wall zone espe-

cially may be almost totally recrystallized, leav-

ing only the outer lamina preserved. Light

luminae are completely recrystallized in one

specimen from Mt Chumbers Gorge, Stylolites

on column margins are yery frequent yt Teatree

O.S., Arkaba Hills and Martin's Well, post-

dating the recrystallizatiow of taminge and

replacement of ooids by sparry calcite, but

apparently pre-dating dolamitization. Local

large sGulion cavities are rimmed wih zoned

ferruginous Uolomite rhombs, then Filled with

course. Branvlar sparry calcite.

Comparisons

The stromatolites are characterized by w very

wide varialion of gross morphology, especially:

branching, which distinguishes then from all

parallel-branching stromatolites, although some

resemble Inzeria Krylov in having deep inden-

tations into the main column at branching,

They are assigned to the group Tungursia on

the presence of imarkedly divergent branching,

subhorzontal columns, and thus differ from

the other divergent branching groups Linella

Krylov, Baicaia Kryloy, Anahbaria Komar,

Poludia Raaben and Parmitex Raahen. Linefle

hus very numerous pointed projections, and

columns are subhasizontal only in the marginal

portions of bioherms. Baleulie differs in having

chiefly ragged, unwalled, margins, with fre-

quent overhanging Taminae. Anubaria has con

sistent, slightly Wivergent branching, and cylin-

Urical columns, The columns of Paludia are

complexty curved ond intertwined, while those

of Pormites are anastomosing.

Tragessia etine differs from all other forms

of the group in ity great variation of branching

style, and its microstructure. Some specimens

closely resemble Tunpessfa inne Walter in hav-

ing aolitic, wavy laminac, but TL etlira is uis-

tinguished by its distinct thicker, pinching and

swelling lamination and variable branching.

Diswipution: Etina Formation and equiva-

lents, Umibcratana Group, Central and

Northern Flinders Ranges: Rakcanoona For-

mation at Mt Chambers Gorge: Wunduwi¢

Limestone at Teatree O.S,; Etina Formation

near Blinman, Martin's Well, the S.E. flank

of the Enorama Diapir. Enorama Creck and

the Arkaba Hills area-

Age: Late Adelaidean, cormelated With Lhe

Late Riphcan or Vendian of the USSR,

Tongussia vilkatanna f. nov.

FIGS. dc4, Se, be, 12b-«

Marertal: Five specimens (rom Depot Creek

und Mundallio Creek.

Holotype: S412 (Figs. 4f,12e), Depot Creek.

Name: After Wilkatanna H.S., & km nornthe

west Of the type localily,

Diagnosis; Tungussia with smooth to pently

bumpy suheylindrical to tuberous, frequently

walled columns, with markedly divergent mil-

tiple branching and continuous thinly banded,

hentspherical laminae.

ent ol Mines

Departny

SOLVH AUSTRALIAN STROMATOLITES Ul

Deseriprion

Mode of Occurrence: The stromutolites occur

in pale pink to white pure dolomites und pos-

sibly also ih datk grey dolomites, as extensive

bidstromes, 0,3-2 m thick, interbedded in lami-

nured siltstones and shales. ‘The upper surfaces

uf biwstrames are irregular, undulating, and in

places. erosional, Stromatolitic columns arise

from fatdomimated or cumulate buses (Fig.

l2c), growth frequently commencing upon the

vroded surface of the underlying shale, In some

beds, only the flatlaminated or cumulate

stage of growth is atlained, in others, up to 2 m

thickness of columns develops. Columns are

either bridged aver at the top by laterally

ligked hemispheroids, or eroded. Columnar

portions may grade laterally alone the bio-

strome into laterally linked hemispheroids,

Colume Shape and Arrangemet; Columas are

subcylindrical to tuberous, humpy, 2-10 cm in

diain,. with low broad swellings and constric-

tions; portions of columns widen rapidly above

aconsini¢tion (Fig, 40,d.f). Cross-sections vary

From subeircular lo highly lobate, The orienta-

ton of columns is highly variable, both hori-

zontal and vertical columns being common.

Individual columns are 5-20 em high, but the

whole sttucture muy attain u height of 2 m.

franching: Both vertical colunins and broad

cumule may arise from the Mat-laminated base.

These typically give rise to a number of hon-

zontal columns, from which in tum cither vee-

fical columns branch upwards, or the hori-

zontal coluimns themselves turn sharply up-

wards (Fig. 4e-4), Columns are frequently

consinicied at branching, and then expand up-

wards tuptdly. Multiple, markedly divergent.

branching from one point ig cammen.

Margin Strnerures The lateral surface bears.

numerout broad bumps of up to several centi-

metres (Flg, 4c), but in places columns are

quite smooth (Figs. 4f, 12e}). Overhanyging

laminae pte relatively rare, and any peaks and

cornices present are only a few millimetres long

(Fig. 461, A wall is usually preseny but may

he absent: unwalled areas are relatively smooth

of finely fringed, the laminae abutting against

the columA margin at varus angles (Fig,

12b,u1, In walled areas, the Jaminae gradually

thin and cover the surface for a distance of up

lay

fo 1 em. The wall varies jn thickhiess Lrom |

to 10 Jaminae (Fig. 12e). Bridges became pro-

minenl near the top of the structure.

Lamina Shape is mostly hemisphericul, bul

gently convex Jaminae occur in wide columns

and in some horizontal columns, especially in

unwalled portions. Laminac are smuothly

curved, without sharp flexures, their shape

being inberited from underlying laminge.

Micro-unconformities occur, but are mostly

only slight, Fig, Se illustrates some representa-

tive Jamina shapes. 83% of laminae have h/d

between 0,2 and 0,5, the mode (33%) being

between 0.3 and 0.d (Fig. Ge). In places lami-

hae develop two crests, anticipating branching.

Near the margins of columns, laminge thin.

and gither abut against the margite (in places

eroded) wr bend over to farm 4a wall, Laminae

are either amooth or very gently wndulating,

with amplitude not exceeding one millimetre.

Micrasieucture is best preserved in silicified

portions of colamos; it is finely banded, con-

sisting Of alternating (hia continuous dink and

light luminue; continuity is broken only hy

micro-unconformities (Fig. 12e}, In the less

well preserved dolomitic stromatolites. the

finest latdinue are frequently obliternted and

macrolamimnae lend to predominate (Big, 1b).

Light fuminee vary in chickness from 0.05-0,2

mm, most commonly 0.05-0.1 mm, bur thin

towards the column maryins where they form

the wall. The upper and lower boundaries are

parallel, and usually distinct and smooth. Na

unequivocal detrital grains were scen; some

thicker pale laminae are of finely grumous tex-

ture. representing parttally recrystallized dark

macrolaminae. Well preserved light laminae in

silicified columns consists of extremely fine

lransparent chert—u xAcnowpic aggregate of

equidimensiona!l quuitz grains, 0.001-0.01 mm

in diam. Where preserved as carbonate, the

light laminae consist of xenotopic ta fypidin-

topic dolomite uf cquidimensional 0.005-0.02

mm erains. Dark feminee are generally thinner

than Jight laminge (0.02-0.2 mm, most com-

monly 0.02-0.08 mmm). Where well preserved

they have smoath. distinct boundaries. and are

quite continuous, but jn parts of dolomitic

columns, they are preserved only as chains of

elongated lenses, 0.1 to 0.5 mm long (Fig.

Fig. 4. Reconstructions of Tinipussa efiea und T'vnsassia wilkatanna. (a, b)—Tungussia etina, Holo-

type $435, Balcanoona Formation, near Mowat Chamibers; (c-7)—Troenssia wilkotanna, Skil-

logalee Dolomite, Southern Flinders Ranges; fc, t)—S169. Depot Crock: (d)—S323, Mun-

dallio Creek; (€]—S410, Depot Creek; (f|—Holotype. S412. Depot Creek: (g}—S408, Depot

Creek; (1) S209, Depart Creck.

A. Deponmont of Miner

7i-P ida

Tig. 5.

Examples of Lamina shapes of stroma-

tolites, traced from thin sections, (it) —

Linea ukkay (b)—Linella mauayallina;

(e)—Qmachtenia utschuriea: (d)—Tun-

sussia efina, (e)—Trngyssta iwilkatanie

un de

BA Deapersirentoal [sme

Frequency distribution of Jamina con-

vexities for stronratolites illustrated in

Fig. 5

W. ¥. PREISS

126). Silicified dark laminae consist of

extremely fine, pale brownish-yrey organic

stained chert, of grain size 0,00)-0,005 mm.

Carbonate laminae consist of xenotopic dolo-

mite of equidimensional 0,003—0,005 mm

wrains. Macrolaminae, 1-3 mm thick, coastst-

ing of up to 10 light-dark lamination puirs,

occur only in the dolomitic portions of columns

(Rig. 12b). In plages, the fine internal lamina-

tion of macrolaminae is obliterated almost

entirely, but these grade laterally into unaltered

light and dark, very thin Jaminae,

Interspaces: The distances between. neighbour-

ing columns vary from several millimetres to

several centimetres. The interspaces are filled

with almost completely unbedded intraclast

wackestone, Clasts vary from 0.5-2 cm; most

are wel! rounded, and compoxed of homo-

geneous dolomicrite. Some are partially recrys-

tallized to grumous-textured dolomite. Long,

Nat intractasts. O.5-1 mm thick, up to 2 ¢m

long, are common near the buse of one speci-

men; these ure commonly replaced by coarse

sparry hypidiotopic dolomite. Intrachasts are

randomly oriented, looscly packed and gene-

rally matrix-supported.

Secondary Alteration. All definitely identified

ovcurrences ure found in pale pink to White

dolomites; other specimens from dark grey

Uolomites at Depot Creek probably also belong

to this group but are inadequate for reliable

identification. The dolomite generally preserves

most fine structure (as does the Skillogalec

Dolomite of many other areas), but in places

id significantly recrystallized. Silicification of

portions of columns occurred after the growth

of whole columns, but before partial alteration

of the surrounding carbonate, since it best pre-

serves the finest lamination. In places it is pos-

sible to trace unaltered very thin laminae from

silicified to carbonate portions of columns; in

the Jatler, only broad light and dark macro-

liminaeé are preserved, The dolomitie nature of

the whole (unsilicificd) sediment suggests

either penccontemparaneous dolomitization

(during siromatolite growth) or trapping ol

dalomitized lime mud, Silicifleation therefore

probably post-dates dolomitization. Grumous

lextures. are developed sporadically throughout

stromatolite and interspace sediment, and were

probably formed by partial recrystallization

during later diagenesis. Irregular stylolites. buth

culting columns and following column margins.

post-date the development of grumous texture.

They are commonly rich in linvonite, and, in

Places, pale green chlorite.

SOUTH AUSIRALIAN STROMATOLITES UE

Compurisons

The stromatolites ate assigned to the group

Tungussia on the basis of their multiple,

markedly divergent branching and frequent

horizontal and. gently inclined columns, These

Characters, in addition to @ cansistently

smoother murgin structure and frequent pre-

sence Of a wall, distinguish them from Boaicalta

burre which occurs elsewhere in the Skillogalee

Dolomite. Tungussia wilkatenna js dilfcren-

Hated from T, nodosa Semikhatoy by its

smoother column margins, smoother, consis-

tently hemispherical and never disharmonic

laminae. It resembles 7. sihiriea Nuzhnoy in

having numerous horizontal columns with up-

turned ends, but is distinguished by its

smoother margin and presence of a wall. 7.

wilkafanna is distinguished from TT. bassa

Krylov in lacking long horizontal columns, and

in aceurring independently, not as a fateral

variant of Linelle wkka Krylov. Unlike 7:

erecra Walter. it lacks long erect columns, and

is distinguished from Ty inne Waller by its

smooth laminae. T. wilkata@ina most closely

Tesembles T, confuse Semikhutav, but is dis-

tinguished by its thinner, more continuous lami-

201

nac of predominantly hemispherical shape. 7.

wilkatanma has more regular and discrete

columns of constant! shape and branching than

T. efina, and has thinner, more continuous,

smoother larninae.

Distribution: ly the lower third of the Skillo-

galec Dolomite, Burra Group; South-western

Flinders Runges: Depot Creek and Mun-

dallio Creek. Small specimens possibly to be

included, come from near the base and near

the lop of the formation,

Mye-> Early Adclaitean.,

Acknowledgments

1am indebted to Prof. M, F, Glaessner for

supervising this study, to the support given by:

the Centre for Precambrian Research, Univer-

sity of Adelaide, and to Dr M. R. Walter Por

discussions and collaboration, Messrs. B.

Murrell und N. S. Pledge kindly supplied me

with specimens, and Mr R, P. Coats indicated

several stromatalite loculities, Drafiine hy the

Drafting Branch, Department of Mines, and

by my wife is gratefully acknowledged. This

puper is published with the permission of ihe

Director of Mines.

References

KHOMENTOVSRIY, V, Vu, SHENTIL'. Vo ¥.. YARSHIN,

M. S.. & Borakoy, BE. P. (1972)-—"Opornye

ragrezy ollozhemty verkhnego dokembriyn i

nizhnego kembriya sibirskoy — platformy”

(“Standard sections of Upper Precambrian

and Lower Cambrian deposits of the Siberian

Plinform”) (Publishing House “Nauku">

Mauscow.)

kKoroLyuk, LK. (1960).—Stromatolity nizhnego

kembriya i proterozoya Irkutskogo amfiteatra

(Stromatolites of the Lower Cambrian and

Proteruzoie of the irkut Amphitheatre.)

Trudy fast. Geol, Razah, Gasyuelh. tsheip.

Akad. Nawk SSSR WV, 1-161.

Keypow LON, {1967} Riteyakls 1 nizhne-kem-

briyskie stromatolity ‘lyan’Shanya i Karatau,

(Riphean and Lower Cambrian stromatolites

of Tien Shan, and Karatau), Fruedy geol. Inset.

Leniagr., V7, 1-76.

NuvHnoy, 8S. V. (1960),—Stromalolily poxdnedo-

kembriyskikh i kembriyskiskh otlozheuiy vos-

tochnykh sklonov Aldanskogo — Shchita.

(Stramatolites of the late Precambrian und

Cambrian deposits of the eastern slapes of

the Aldan Shield.) Dokl. Akad. Nauk SSSR

132(6), 1421-1424,

NuzHnov, S$. V. (1967).—Rifeyskic otlozhentyu

yugo-vostoka sibicskoy platformy. (Riphean

deposits of the southeast Siberian, platform.)

Inst. Geol, Yakuisk. Filial Sibirsk. Otdel.

Akad, Nauk SSSR; Moscow, 1-160.

Preiss, W. V. (1972).—The systematics of South

Australian Precambrian and Cumbrian Sto-

matolites, Purt 1. Trans, R, Soe So Aayr. 96,

67-100.

Preiss, W. V, (1973a).—The systematics of South

Australian Precambrian and Cambrian stro-

piste Part UL. Yrany. R. See. §. Aust, 97,

1-125.

PREiss, W. VY. (1973b).—Palavogcologica! inter-

pretattions of South Austratian Precambrian

stlromatalites, J, geal, Soe. Aust. 19, 501-532.

Sesoeiatov, M.A. (1960) —O vertikal'nom rus

predelenii stromatolitov y rifeye Turukhan-

skugo rayona, Dekl. Akad. Nawk SSSR 135

(6), 1480-1483.

SEMIKIATOV, M, A. (1962)—Rifey | fizhniy

kembriy = Yeniseyskogo Kryazhs. (The

Riphean and Lower Cambrian of the Veniser

Mountains | Trady. geol. lst) Leniner. 68.

1-242.

Wactex, M. R, (1972).—Stromotolites aud the

hiostratizraphy of the Australian Precambrian

and Cambrian, Palaeontology, Spee, Paper M1,

1-190, 33 pls.

202

Fig.

10.

W. V. PREISS

Linella wkka, Balcanoona Formation, Burr Well, Northern Flinders Ranges. (a)—Longitudinal

sections of tuberous columns with pointed projections in outcrop. Marking pen is 10 cm long;

(o)—Longitudinul sections of inclined columns at a bioherm margin. Diameter of lens cap is

§ cm; fc)—Cut slab, showing divergently branching columns. The while areas ate patches

of coursely crystalline calcite. $478; (d)—longitudinal thin section (S477); Laminae are

largely obliterated by recrystallization; (¢)—A cut. slab, adjacent to thin section in (d),

Linella munyallina, Wundowie Limestone Member, Northern Flinders Ranges. (a)—Recurvyed

margin of a bioherm, lowest Jimestone band, Burr Well; (b)—Longitudinal sections of com-

plexly branching columns, Rocbuck Bore: (¢)—Inclined columns at a bigherm margin. Lowest

limestone band, Burr Well; (d)—Outcérop of a small bioherm. Lowest limestone band, Burr

Well; (e)—Thin section inclined columns from a bioherm margin. Here the wall is poorly

developed, Vowest limestone band, Burr Well. 5486; (f)—Thin section of columns with

numerous bridges, Munyallina Valley, S294.

(a-c)—Linella munyalling, Wurdowie Limestone Member. (aj)—Thin section of slightly

divergent branching columns, Roebuck Bore. S431; (b)—Thin scetion of holotype, $495,

showing steeply domed laminae in parallel, walled columns, Note sandy lenses in the inter-

spaces; (c)—Thin section of slightly divergent branching columns. West Mount Hut, $555;

(d)—Oniachtenia ulscharica, outcrop, uppermost beds of the Tapley ill Formation, Depot

Creek: (e)—As for {d), showing numerous bridges between columns.

{a-c)—Longitndinal thin sections, Omachtenia uischurica. C(ay—Dlustrating pelletal lamina-

tion and coarse intraclasts in interspaces, $166, Depot Creek; (b)—Iustrating details of pel-

fetul microstructure. $399, Depot Creek; (c)—-Illustrating broadly banded microstructure; (d,

e)——Tungussia etina; (d)—Longitudinal outcrop section showing markediy divergent branch-

ing, Balcanoova Formation, neat Mount Chambers; (e)—Onutcrop of irregularly tuberous

columns, Etina Formation, Enorama Creek.

(a) —Tungussia etina, Umberatana Group, Flinders Ranges, Longitudinal cut slab showing

markedly divergent branching of columns. Wundowie Limestone Member, near Teatree O.S.

$441; (b)—Longitudinal thin section of walled columns, Wundowie Limestone Member.

near Teatree O.S. 8446; (c)—Vertical thin section of variously oriented columns, Balcanoona

Formation, neat Mount. Chambers. Holotype $435; (d)—Wavy, banded lamination seen in

thin section, Etina Formation, east of Blinman, 5158; (e)—Longitudinal thin section, HKal~

canoona Formation, near Moiint Chambers, $525.

. (2)—Longitudinal thin section, Tungussia etina, Wundowie Limesione Member, near Teatree

OS, $286: (b-c)—Tungussia wilkatanna, Skillogalee Dolomite, Depot Creek, (b)—Longi-

tudinal thin section illustrating sharp flexure in column. S169; (c)—Outerop of bushy, diver-

gently branching clump of columns: (d)—Cut slab, S169, illustrating markedly divergent

branching; (e)—Thin section, holotype 5412, showing markedly divergent branching columns.

White arcas are silicified.

SOUTH AUSTRALIAN STROMATOLITES Il 203

W. V. PREISS

204

Fig. 8.

SOUTH AUSTRALIAN STROMATOLITES IIL 205

SOUTH AUSTRALIAN STROMATOLITES III 207

SE,

2 cm

Fig. 11.

W. V. PREISS

208

Fig. 12.

AMPHIBOLURUS GIBBA, A NEW DRAGON LIZARD

(LACERTILIA:AGAMIDAE) FROM NORTHERN SOUTH AUSTRALIA

BY T. F. HOUSTON*

Summary

HOUSTON, T. F. (1974). -Amplibolurus gibba, a new dragon lizard (Lacertilia: Agamidae) from

northern South Australia. Trans. R. Soc. S. Aust. 98(4), 209-212, 30 November, 1974.

A new species of agamid lizard is described and figured. It is regarded as a member of the

Amplibolurus reticulatus species-group and shows close affinity with A. maculosus (Mitchell).

It appears to be confined to the gibber plains of northern South Australia.

AMPHIBOLURUS GIBBA, A NEW DRAGON LIZARD (LACERTILIA:

AGAMIDAE) FROM NORTHERN SOUTH AUSTRALIA

by T. F. Houston*

Summary

Houston, T. F. (1974).—4mphibolurns gibba, va new dragon Jizurd (Lacerulin; Agamidae)

from notthern South Australia. Trens. R- Soe. S. Aust. 98(4), 209-212, 30 November,

1974.

A new species of agumid lizard is described and figured. Wt is regarded as a member of the

Anphibolurus reticulatus species-group and shows close affinity with A. miaeulosus (Mitchsll).

Jl appears to be confined. to the gibber plains of northern South Australia.

Introduction

The species described herein as. new is a

lille known inhabitant of ihe barren, stone-

strewn gibber plains of far northern South

Australig, Specimens have been received at the

South Australian Museum over the past 27

years bur were variously misidentified. most

of them as Amphihbolurus imbricatuy Peters

(=4. ¢, caudicinenis (Gunther)—Storr 1967).

Mitchell's (1955, p. 387) reference to the

necnrrence of A, inthrivatis near Marree und

Finniss Springs, S. Aust., was based on these

apecimens,

Enquiries by the present author revealed

one specimett in the National Museum of Vic-

toria, Melbourne, but none in other Austra-

lian museums. Except where indicated other-

wise, all specimens listed below are in the

South Australian Museum. Afl localities men-

tioned are in South Australig.

Amphibolurus gibba n.sp.

FIGS. 1-4; TABLE 1

Holotype: 2. RiZ9S4A, 5.5 km NNW. of

Alberrie Creck Railway Siding, S. Aust.

(29°35'S, 137°31'E), 14.7974, ex burrow

under cracked mud crust of gibber plain, R.

Forsyth & T. Houston,

Diagnosis: Agrees with A, reficulatus (Gray),

A, inermis (De Vis) and A. maculosus

(Mitchell) in general form (short decp head.

abrupt profile, denticulate eye lids, smooth-

scaled back and relutively short tail), Agrees

with A. maculosns, but not A. reticularus and

A. inermis, in having nostrils situated below

* South Australian Museum, North Terrace, Adelaide, 5. Aust. 5000.

Hos

®Conber Pady

Fig. t. Map of north-eastern South Australia

showing collection localities (solid

squares) of Amphibelurus gibba,

(not On) canthus rostralis. Differs from the

three in having relatively longer hind limbs

(mean tatio of Ieg Jength to snout-venl length

=81%; cf. 57-67% in other species): femoral

and preanal pores (mean — 30) more

numerous thon in 4. ineroms (21) and A.

maculosus (10, femoral only) but fewer than

in A. reticulatus (37); ear openings relatively

smaller than in 4. rerculams and A. inermis

but not scale-covered as in A. maculosns. Dis-

210

linguishable also by coloration: throat with

conspicuous round black patch {with dark

reticwum in A. redicu/aras and A- inernis; with

Jongitudinal black strenk jn A- mtacnlosus);

chin with median black streak, back butt to

jurra-cotra ted, offen darkly speckled, usuully

with &—-8& pairs of blackish paravertebral spets

(with blackish reticulum in adult A. resiculatius

and 4. inerniix; white to grey in A. macitlosay

with bolder paravertebral spots); tail with

linear series of 2630 dark spots each side

(absent in other species).

Description: Stout, moderate-sized dragon

lizards reuching a snout-vent Iength of 82 mm

and total Jength of 190 minty. head relatively

short and deep; snout obtuse, rising steeply in

profile; nostril situated helow slightly swollen

canthus rosttaliss ear aperture relatively small

und elliptical; body depressed: fore limbs

relutively large, reaching or almost reaching

groin wheo adpressed; hind limbs moderately

long; til anoderately long and evenly taper-

ing. «(See Table | for proportions}, Tn juveniles

the head und appendages are relatively longer

than in adults.

TABLE 1

Howlv proportions expressed as percentaye roties jer

spectnens af A, gibba with « seentvent length of 53

nom or nlere

(n — sample sims ro > range, im mean, 2 =

standard devialion)

Propoction n 7 m 5

Hond Jonsth: SVL oi 2642 30a

Head width: Jena 1 ASRS 35 As

Eur diameter bead width 15 16-21 18 is

Dore timh lane: SYL 14 39-48 3B pu |

And limb teneth. SYL 14 75-90 3! a8

"Vall leoeth: SYL 12 i121 54 133 78

Dorsal scales of head weakly lu stronely

convex, angular, transversely carinate or ridged

in front of and behind supra-orbital jreus; a

sow of enlarged, longitudinally ridged or

carinate scales from belew eve to above ear;

outer margin of lower eyelid fringed with s

row of very acute scules; 4 seale rows

separating nasals from upper labials; 12-17

upper Jabial scales each side; temporal, occi-

pital, nuchal and axillary scales very small and

convex, Interspersed on the head (sometimes)

with a few spinous tubercles; no nuchal crest

but a few median scales slightly enlarged;

seales on temainder of body, Jegs and tail

(dorsally) flat ind smooth, those of the buck

largest medially; keels appearing only on yen-

Iral side of tail, strongest distally; 26-395

T. F, HOUSTON

{mean ~- 30) femoral and preanal pores well-

spaced along a fairly straight Jine extending

full length of each thigh; each pore surrounded

by several scales, those anterior to it being

slightly enlarged.

Dorsally grey to buff-brown, tinged in some

indivadwals with pink or lerra<otts; cach side

ef head with 3—+ ultermating light and durk

vertical bars from eye to lower lip (sometimes

faint); back with 6-8 pairs of blackish paru-

vertebral spots from) shoulders to rump; simi-

far §pors sometimes present on fanks; tail with

20-30 dark blotches along ench side; chin

with a small black median streak and throut

with a large median black patch) chest with it

faint grey to intense black patch medially, The

holotype, in life, had a fight yellow wash

across the anterior part of the chest and

shoulders,

Measurements of heletype (in mm); Head

lenvth, 21; head width, 16; maximuny diymeter

of cur, 2.8: snout-vent length, 72; fore Jimb

length, 34; bind limb length, 58; teil length,

100.

The specific epithet, taken fram Cooper's

41949) Hist Of Aboriginal words and mean-

ing desert stone or rock, is used as a2 neun in

apposition and is mot subject to termination

changes,

Specimens examined: Puralypes: same dita as

the holotype, R13954B-K; 34 km N af Coober

Tedy, &. Story, 6.6.1973, R13983; 37 km 3 of

Coward Springs on oad to Stuart Creek H.S,,

‘gibber, crumbly clay sail, ran into burrow”,

Zoology Dept.. University of Adelaide,

26,%,1969, Rt1165; Finniss Springs, 4. /.

Pearce, 174.1947, R525, RI3894A-B: same

loc, Food Mitchell, 641.1964, RISAYI Lake

leltte Waterhole, G. F. Gress, 23411956,

R3I805; Marrece, F. 2 Mitchell, June 1 9n6,

R9499; 3,2 km § of Muttea, FP. J. Mitchell,

Feb. 1966, R7605—-6, R8310: 14 kin SPoot Mt

Hamilton Stn on Mirguret River, R. Tedjorel,

19.¥.1953, R3542; 32 km N of Oodnucdatea, J,

Bredl, 197L, RI2494A4-B; Johnsons Bore track

midway hetween William Creek and the

Neales, 23.viil,1969, Nut, Mus. Vie. 039937,

Systematic position

The genus Aniphiboluruy Wagler, as it cure

rently stands, contains many diverse clements

and no satisfactory definition of it is pvailable.

Iis species cohere more by the lack of

specralized features characterizing alher genera

than by possession af features unique to then

as i group.

NEW DRAGON LIZARD FROM NORTHERN SOUTH AUSTRALIA 211

Figs. 2-3. Anterior and lateral views of holotype of Amphibolurus gibba in life.

Fig. 4. Juvenile of A. gibba in life.

212 T. BL HOUSTON

The placement of 1. gibba in Amphibolurus

is based on its apparent affinity and close simi-

lurity io species (4, reyienlatus and Ay inernis)

lony placed in this gents.

in the totally of its features, A. vibha ws

intermediate between A. reficulatus and A,

inermis on the one hand and A. macnlesuy on

the other. Structurally it most closely resembles

A. retienlatus but in size, nostril position and

coloration iL approaches A. miaculostis, The

latter species was originally included in the

genus Tvipanacryptis Peters (Mitchell 1948.

Storr 1964) on account of its scale-covered

cars bul was subsequently removed to Aimphi-

holneuy on the basis of osteological evidence

(Mitchell 1965). Closure of the ear openings

was believed to be a secondary development.

I support Mitchell's conclusions und sug-

gest that 4. ynacilosus and A, gibba are

derived from a common ancestor and that the

covered cars of the former evolved through an

intermediate stage such as is now seen in 4.

vibba,

T also suguest that A. gibha and Al. muicu-

losuy be regarded as members of the A. reticu-

latus species-zroup (Storr (966). although my

conception of this group does not extend to

include A, decresii (Dumeril & Bibron) or a.

pictus Peters (see Houston 1974, pp, 57-58).

The species-group as understood here contains

habitual burrowers in which sexual dichroma-

lism is either not evident or only feebly

developed.

Acknowledgments

fam grateful to Mr. M, J. Tyler, Honorary

Associate in Herpetology. South Australian

Museum, who sought specimens of the new

species on my behall curing visils Lo lwo Aus-

tralian Museums, to Mr, Ross Forsyth who

energetically assisted me in field collection.

and to Mr. A. J. Coventry, Field Olicer,

National Museum of Victoria, Melbourne. for

providing a specimen for study.

The distribution map (Fig. |) was prepared

by Miss Adrienne Edwards.

References

Cooprr. He. M. (1949). Australian Aboriginal

words and their meanings”. (South Austra

lian Museum: Adelaide.)

Houston, T. F. (1974).—Revision of the slmphi-

holurus — decresii complex (Lacertilia:

Agamidae) of South Australia. Trasis. KR.

Soc. S. Aust. 98(2), 49-60.

Mircneit, F. J. (1948).—A revision of the Jacer-

tilian genus Tympanocryptis. Ree. S. Aust.

Mus. 901), 57-86.

Mricuet.. F. J. (1955)—Preliminary account

of the Reptilia and Amphibia collected hy the

National Geographical Society —Common-

wealth Governmest—Smithsonian Institution

Expedition to Arnhem Land (April to

November, 1948). Ree. S. Aust Mus. 104),

373408.

Mrrenent, Fed. (1965).—The aliuitics of Tyan

panocryplis macilosa Mitchell (Lucertili-

Agamidae). Rec. S. Aust. Muy, 15(1), 179-

191,

Srorr. G. M. (1964),—The agamid lizurds of

the genus 7 veipanecryptis in’ Western Aus

tralian. J. R. Soe, West. dust, $742), 43-350,

Store. G. M. (1966).—The Amphibolurus reticu-

latis species-group (Lacertilia. Agamidae) in

Western Australia, J. R. Soe. West, lust.

49(1), 17-25.

Storr, G. M. (1967).—Geographic races of the

ugamid Jizard Amphibolurus vasdicinctus, J,

R, Soc. West, dust. 50(2), 49-56,

A REVISION OF THE FOSSIL MEGAPODIIDAE (AVES),

INCLUDING A DESCRIPTION OF A NEW SPECIES OF PROGURA DE VIS

BY G. F. VAN TETS*

Summary

VAN TETS, G, F. (1974) .-A revision of the fossil Megapodiidae (Aves), including a description of

a new species of Progura De Vis. Trans. R. Soc. S. Aust. 98(4), 213-224, 30 November, 1974.

Long bones of two fossil species of megapodes are described from Pleistocene deposits from

south-eastern Australia. Both species are much larger than extant species of megapodes. The larger

of the two, Progura gallinacea De Vis, 1888a, was described and classified as a crowned pigeon,

Columbidae; as an undetermined bustard, Otididae (De Vis 1888b); as a megapode, Chosornis

praeteritus De Vis, 1889; and as a stork, Palaeopelargus nobilis De Vis, 1891.

The smaller of the two is named Progura naracoortensis n. sp. It differs from its congener by

having a relatively shorter tarsometatarsus.

Of other megapodes, fossil remains have been found only of one specimen of Leipoa ocellata,

Malleefowl, and of one or more indeterminable juvenile megapodes. Fossil remains reported as

those of Alectura lathami, Brush-turkey, are of Progura gallinacea and P. naracoortensis.

A REVISION OF THE FOSSIL MEGAPODIIDAE (AVES), INCLUDING

A DESCRIPTION OF A NEW SPECIES OF PROGURA DE VIS

by G. F. yan Trers*

Summary

van Ters, G, F. (1974)—A_ revision of the fossil Megapodiidae (Aves). including a descrip-

tion of a new species of Pregura De Vis, Trans. R. Soe. S. Aust. 98(4), 213-224.

30 November, 1974,

Long bones of two fossil species of megapodes are described from Pleistocene deposits

from south-eastern Australia. Both species are much larger than extant species of megapodes.

The larger of the two, Progura gallinacea De Vis, 18888, was described and classified as a

crowned pigeon, Columbiduc; as ah undetermined bustard, Otididuae (De Vis 1888b); a5 a

megupode, Chosarnis praeteritis De Vis, 1889; and as a stork. Palaeopelareus itohilis De Vis,

1897,

‘The smaller of the iwo is named Progura naracoertensis 1. sp. Tt differs from its congener

by having a relatively shorter tarsometatarsus.

Of other megapodes, fossil remains have been found only of one specimen of Lefpoa

ocellata, Malleefow!, and of one oy more indeterminable juvenile megapodes, Fossil remains

reported as those of Alectura lathami,

PB. naracoortehsis.

Introduction

Brodkorb (1964, p, 307) mentions only two

fossils in the Megapodiidae, a carpometacarpus

which is the holotype of Choyernis praeteritus

De Vis, 1889, and a coracoid which Lydekker

(1891) determined as that of a Jarge gallin-

accous bird and provisionally referred to Alec-

mare farhami J. BE. Gray. 1831, Brush-turkey.

A tarsometatarsus, closely comparable with

that of A. dathaml, was reported by Longman

(1945),

Recently more fossil material of megapodes

was locited in south-eastern Australia, mclud-

ing remains of an undescribed species. “hese,

and four tarsometatarsi, the syntvpes of Pro-

gura gallinacea De Vis, 1888a, are here re-

assigned to the Megapodiidae. Progura was

placed by De Vis in the Columbidae néar ihe

crowned pigeons (Goura Stephens, 1819),

De Vis (1888a) considered both Progura and

Goura to be close to the common uncestor of

poultry and pigeons.

In this paper the new species is described,

and the long bones of fossil megapodes arc

compared with those of extant megapodes

(Megapeditis pritchard’ G. R. Gray. 1864,

* Division of Wildlife Research. CSIRO, ?.0. Box

Brush-turkey,

are of Progure gallinacea and

Niuafou Fowl; MM. (jreycinet) retnwaret

Dumont, 1823, Scrubfowl; Alectura Jathami,

Brush-tturkev; and Lelpoa ocellata Gould,

1840, Malleefow!); and of crowned pigeons

(Goura scheepmakert Finsch, 1876, and G.

victoria (Fraser, 1844)).

Methods

‘The study material was made available by

the following museums and is identified in the

text by their initials and numbers; Australian

Museum, Sydney {AM); British Museum

(Natural History), London (BMNH);

Nations] Museum of Victoria, Melbourne

(NMV); Queensland Museum, Brisbane

(QM); South Australian Museum, Adelaide

(SAM); United States National Museum,

Washington (USNM): and CSIRO, Division

of Wildlife Research, Canberra (CSIRO).

The terminology of Harvey ef al. (1968)

is used for bones and their parts. Examples of

fossil bones are figured together with a corre-

sponding bone of a Scrubfow]. Mirror images

of some bones have been drawn, so that all

bones on a figure appear as if they are From

the same side.

&4, Lyneham, A.C.T. 24602.

214

Measurements of the bones wete made as

recommended by Scarlett (1972) and Schnell

(1970) aind as indicated on the figures. They

include: length; width at proximal or dorsal

emi, width at arrowest point on shaft; and

wiuth at distal or ventral end. On the carpo-

meracuepus, the greatest and least width of the

proximal end was measured in accordance with

De Vis (1889), and ihe greatest and least

width at the narrowest point on the shaft of

mitacyrpul IMT. On the tarsometatarsus, the

width below the articular impression of the

first metatarsal of bullux and the width of the

central trochlea was measured. On the scapula

the width of the blade was measured,

Weights of Malleefowl were obtained from

the records of the CSIRO Bird-Banding

Scheme, and weigits of Serublowl from the

labels on specimens in the collections of the

Western Australian Museum, Perth und the

Division of Wildlife Research, Canberra.

Material and Synonymy of Mrogare gullinuced

Proeura gallinacea De Vis, 1888: 171-

Chesornis proctertius De Vis. 18897 35,

Pufacepelaraus nobilis De Vis, 1891: 441 (new

s¥nonymy).

The syntypes of Pregura gallinaced De Vis,

18880, are those De Vis figured on Pline VI,

we proximal parts of deft tarsometatars

(OM, F134 and F143) and two distal parts

of rivht tursometatursi (QM, F5556-7).

Becuuse the syntypes are complementary frag

ments of the tarsormetitarsus IT huve nat selec-

ted u lectotype,

De Vis (1889) in his deseription of the

holotype of Chosornis praerecitus, tefers to

“the metacurp of the left manus”, but he

Reures on Plate TY a proximal part of a right

carpomelacarpus which 36 now numbered

QM, Fltt32. Another proximal part of a right

carpumelacarpus bore the same number. bul

has been renumbered QM, F700S, It is more

worn than OM, FLI32 and is nol the one

figured on Plate IV. The deseription vould

perluin to eilber specimen. OM, FLIS2 should

be regarded as the holotype of Chosornis

proeteri¢ux jantl the feference to “the lett

manus” should be dismissed as a lapsis cela,

A ilistal part of a right carpometacarpus

(QM, F1139) is figured by De Vis (1891)

on Plate 24 as the holotype of a stork, Palaea-

pelarguy aobilis, Ciconiidae, Pat Vickers Rich

and Lt found the holotypes of (Aasornis praoe-

leritny and of Paldeopelaraus nebilis (QM,

G, BL van TRIS

Fi132 and FLt39) to be matching Iriagments

of the same bone.

Referred Specimens: The following material

aurees in sige With the type of Progra

vallinaced. In shape. all specimens resemble

the correspontling parts af extant megupodes,

but they are very much larger in size. Progura

gallinecra is the oldest available name for

than. They are: the material of Chosornis

praéteritus (QM, P1132 ant P7005): the

material of Palweopelargns nobilis (QM,

Fli39) smd a distal part of u right wha (QM,

F5553) (referre) by De Vis (1891) }: a prexi-

mal part of a right scapula (QM, F55581

(fizured on Plate 35 and referred to the Ou-

didae as un undetermined venus and species

of bustare hy De Vis (L888b)); an almost com-

plete left coracuid (BMNU, A3244) (Tale-

gulla lathamt 43379 of LvdekRer (1891)); an

almost complete right coracaid (AM,

F54720); a proximal pant of a right ulna

(AM, F54721); distal parts of two right

ulnas (AM, F54722-3)- a proximal purr of a

left tarsometatarsus (AM, F54724); a clistul

part of a left tarsometatursus {AM, F54725))

u distal part of a tight torsometutarsus (AM,

V54726); and an incomplete distal part of a

right tarsometatarsus CAM, F7033). (fonnerly

also numbered QM, F1134).

Description of Prapura narucoenensts D.sp.

Though the following materia} resembles

corresponding parts of extant imegapodes thy

shupe, if ts intermediate in size belween P.

gellimecea anid extant megapades. “The material

is consistent in size. The most distinctive bone

is an almost complete right tarsometatarsus

(SAM. PL7&8563. It is nor only smaller. bul

its relative lenyth is alsa very much shoes

than that of the ayntypes of PL gallindeee,

Hofotype: 1 have tivtefore selected SAM,

P1i7856 as the holotype of Preeare pearn-

coorrensis n.Sp. Iris named afler Naracoorte,

South Australia, where the holotype and

most af the other remains of PL narsceer-

tensiy were found.

Referred specimens: The proximal part of 4

left tarsometatarsus (QM, F2709) was re-

ported by Lonuman (1445) as closely com-

purable with that of 9 Brush-turkey, In size

and shape st looks like a mirror image of

SAM. P1786, the holotype af P. naracoor-

lensis,

Further material of PF. nearecoertensiy con-

sists Of an altnost complete night corucniil

(SAM, PL6700); a complete and two distal

REVISION OF TOSSTL. MEGAPODUDAE (AVES)

ends of left bumeri (SAM, P171534 and

P17878); a proxintal und a distal part of a

right humerus (SAM, P18383); an almosi

complete right ulaa (SAM, P17877); and iwo

distal parts of left ulnse (SAM, P178749 and

PIS182); a complete left radius (SAM,

P18184); a proximal pact of a right femur

(SAM, PL7857): a distal part of a right femur

(SAM, PIS186); a complete right tibiotursus

(SAM. P17152); a distal part of a right tiblo-

tarsus (SAM, P17876); 2 proximal part of a

right tarsometatarsus (SAM. P1S1835): 4 cer-

vical vertebra (SAM, Pi8181); and an an-

terior fragment ol a synsacrum (SAM,

PIBL87),

Fossil remains. of other megapode species

Compared to Progura very few fossil te-

mains have been found of other megapodes.

As axplained above, specimens reported ay

Alechira lathami by Lydekker (1281) and

Longnuin (1945), are also Progure remuins,

and there are no other known fossil remains

oF the Brosh-Turkey,

Fragments of a cranium of a Malleefuw)

(SAM, P16738) were found in the same

deposit with the following temains of one or

more juvenile megapodes of similar size but

of indeferminahle genus and species: a pre-

maxilla (SAM, PIA739), a sternum (SAM,

P16740); a proximal part of a right ulnu

(SAM, P16741); a proximal part of a Jeft

femur (SAM, P'167424: # distal part of a Tight

fenmur (SAM, P16743); a distal part of a Jeft

ubiotutsus (SAM, P1l6744); and an almost

complete night tibiotarsus (SAM. 16745).

Age and distribution of fossil megapodes

The following fossils of megapodes have

been found in Pleistocene deposits in south-

eastern Australia, None have been found in

association with human remains nor with those

of dogs und other domestic and feral animals.

The map (Fig. 1) has been adapted from

Frith (1962),

Souwh-euastern Queensland

The. syntypes of Progura gallinacea (OM.

P1134, F1143 and PS556-7) and £. gallinacea

(QM, F7033) were collected at Ravensthorpe

near =Pillon. Darling Downs (27°54'S.

IS2°WVEI. According to a label associated

with OM, F7033. it was collected on ‘| 1-9-

1888" by R. W. Frost. QM. F1132, the holo-

21s

@ Progura maaccsrlonsr,

WPiogi Salliacee

4 A aipee occliata

OR Mocanodins eewysrt

= Alortwa falhann

£ BeoK "

Fig. |. Distribution of fossil und extant mewa-

podes in Australia,

type of Chosornis praeteritus, and QM, F5559

were, according to labels associated with the

specimens, collected at Chinchilla, Darling

Downs (26°45'S. 150°40'E). The holotype

of Palaeopelargay nobilis {QM, F1139), OM,

F5353 and QM, F7008 are from unknown

localities in (he Darling Downs.

P. naracoortensis (QM, F276%) was

collected on 24 May, 1945. by E, T. O’Roatke

at the Gore Limestone Quarries (28"13'S,

151 30'E) (Longman 1944).

Eastern New South Wales

The first material to be collected of P.

gallinacee (BMNH, A2244), was obtained

from a cave in the Wellington Valley near

Wellington (32°35'S, [48°3SS5°E), and was

presented in {870 to the British Muscum

(Natural History) by the Trustees of the Aus-

train Museum (Lydekker 189)). Another

specumen of P. gallinaewa (AM, F54723) was

collected fram one of the Walli Caves in the

Wellington Valley in 1966 or 1967 by R, M.

Frank', Jeanette Hope found /, 2ullinacea

(AM, P5472N-2, and F54724—-6), in the one

lump of matrix at ihe Wombeyan Quarry of

Industrial Rock Mines Ltd. about 14 km west

of Wombeyun Caves Reserve (34°19°S,

149°56’E), in April 1970. They may be of a

single individual which appears to have fallen

down a Vertical entrance shaft and to have

been crushed by subsequent deposits,

a ee a a Se ek

4 Frank, BR, M. (1972.),—Sedimentolagical and morphological study of selectéd cave systems ip eastern

N.S.W., Australia, PHD. thesis, A-N.U. (unpublished) ,

Z16 (r,

Sourh-easrern South Australia

The holotype of Progura naracoortensts

(SAM, P17856), as well as P. naracoortenxiy

(SAM. P17152-4, P17857, P17876-9, and

PIS181-7) were collected at Henschke’s

Quarry Cave near Naracoorte (37°00'S,

140°45'E) by Mr. F, Aslin. Sample SUA243

from Henschke’s Quarry Cave has a radio-

carbun date of ubout 33,800 BP (N, Pledge.

pers. comm,), P. aaracoortensis (SAM,

P16700) was collected by Dr. R, T, Wells and

othcr members of the Cave Exploration Group

of South Australia at Victoria Cave near

Naracoorte, together with Malleefow! (SAM,

16738) and juvenile megapode(s) (SAM,

P16739-45).

Comparisons of long hones of megapodes and

crowned pigeons

Crracoid

The coracoids of Geurw have relatively

broader dorsal and ventral ends than those of

mevapodes. The coracoids of the species of

megapodes differ mainly in length (see Table

1 and Fig. 21.

Scapula

The scapulae of megapodes and other walli-

form birds have a scapular tubercle. “This

tuhercle does not occur in most other kinds

of birds including Otididae and Goura. The

glennit facet is round in Goure and is quad-

ranpular in Otididae and Megapodiidae. The

long axis of the glenoid facet is parallel to the

shaft id Otididae and at right umgles to the

shatt in Megapodiidae.

The scapula of P. naracoorlensiy ty not

known. The scapulae of the species of mega-

podes differ in size (see ‘Table 2 and Fig. 2}.

Hrmerus

Vhe humeri of Gourw are relatively shorter,

more massive and haye more prominent. cel-

loid crests. ihan those of megapodes, The

humerus of P. gallinacea is. nol known, Tre

humeri of the species of megapodes differ

mainty in length (see Table 3 and Vig. 3).

Ulna

The ulnae of Goura are straighter and have

more prominent feather buses than those of

mevapoudes. ‘The ulnae of the species of mega-

podes differ in size, except for an overlap in

length between Scrubfowl and Brush-turkey

(see Table 4 and Fig. 3),

B. van TETS

TABLE 1

Measurements of Covaccids af Megapndes and

Crowned Pigeany

3 =

£3 2 ¢

2 5 Be.¢ 3

a : » & BL = FI

P. galiluawes BMNH, A3244 1, WW

AM. F54720 RK 04 mW 30

P, naracnoriensis SAM. P16701) KR 85S 18 10 24

G. victoria NMV, W6676 L ok oY 9 35

mR $3 19 9 25

G. sehtemmakerl NMV, RASS tL 7 #49 9 26

R 7 17 & Bf

1, celta SAM, Bilde2 foo 64 14 ff IR

R 63} 12 G 18

SAM, BI4H16 QoL fF 14 6 1B

RK 64 14 f Ww

SAM, f5030 9 L oe 44 6 39

R 24a ow

NMY. Bo276 L 64 WW a 7

Rk bb LF 7 48

Aj Tivtiavol NMV) Wes 1 6h oT no

R oO |) 5 18

NMY, Wa554 bk oe 4 518

R 4 {! 5 tT

NM¥, W4554 lo oon 12 FOS

ROSH oO <9

M. reiowurdi CSIR.

GALS? wt sd it $-31T

ot en a

CSIR,

GALS3 ft 55 WW 5 32

Ross ofl 5 4}

M, writchardi USNM, 319644 Le. 7 » (0

RST ? + WwW)

Radius

The radii of Ganre ave arched Upwards and

those of megapoedes are arched forwards,

The cudii of the species of megupodes differ

in size except for an overlap in length between

Serubfowl and Brush-turkey (sce Table 3 and

Vig, 3),

CUrpormelacar pus

The carpal IL process of Goure is relatively

larger and more prominent than that of mega-

podes. De Vis (1889) noted the absence of

wn intermetacarpal process in the holotype of

Chosornis practeritys. This process is a pro-

minent structure in the Passeriformes arid

the Northern Hemisphere based galliform

families, Phastanidae. Tetraonidae anil

Meleagridae. It is absent in the Columbi-

formes including Goura and the Southern

Hemisphere: based galliform families. Mega-

podiidae, Cracidae and Numididue. The car-

pometacarpus of P. raracoorrensiy is not

known. The curpometacarpi of the species of

REVISION OF FOSSIL MEGAPODIIDAE (AVES) 217

. @, and o—tright carpometacarpus, M4. reitwardt (CSIRO, GALS3); 4, and d.—tright carpometi-

carpus, P. gallinacea (QM, F1132 and F139); &—right coracoid, P. naracoortensis (SAM,

Pl6760); f—right coracoid, M- reinwardt (CSIRO, GALS3); g.—tight coracord, P. galfina-ea

(AM, F54720); hk. and j—right scapula, P. gallinacea (QM, F5558); i. and k,—right scapula,

M. reinwardt (CSTRO, GALS3).

megapodes differ m size, except for an overlap

in length between Scrubfow!l and Brush-turkey

(sce Table @ and Fig, 2),

Syasaerurn

The syosacra of Goura have a median yen-

tral ridge ut the anterior end, This ridge does

not occur in megapodes. The synsacra of

megapodes differ in size (see Fig. 4).

Femur

The shaft is narrowest distally in Gowra and

proximally im megapodes, The trochanteric

ridge is more pronounced in megapodes than

in Craura. The femur of P. vallinacea is not

known, The femora of the species of mega-

podes differ in size except for an overlap in

length between Malleefowl and Brush-turkey

(see Table 7 and Fig. 4).

Tibiotarsts

The tibiotarst of Goura lack a prominent

notch on the medial condyle which is present

in megupodes, The tibiotarsus of P. gallinacea

is not known, The tibiotarsi of the species of

megapodes differ in size except for an overlap

REVISION OF POSSLL MEGAPODIIDAE (AVES)

TABLE 2

Measurements of Sctapulue of Megapodes and

Crowned Pigeohks

s a

E Es 3

u BE =

2 g gaa 5

3 » 3 2 ws Ec

8 z # 2 § £2 82 23

P, gallinscea QM. F5558 R 22 14

G. victoria NMYV, W6676 L & 4 #7 &

R 87 4 #7 OU

G. scheepmakerl NMV. Ra054 Lo oB7 oa 6 12

R oes 12 6 I

R 80 12 fF WW

A. Sathouni NMY, W5964 LC 7 10 5 4

R 7 Ww & ¥

NMYV, W454 Lom Wm 4 9

R 77 t Ss »

NMV, Wa5s5 Law 9 5 8

R 7% Ww Ff 8

M. reluyracdt CSIRO,

GALS 2 gd il we 9 F &F

68 10 7

CSIRO,

GALS3 a Rk 8 9

lat

a oa

M. pritchardt USNM, 319634

in Iength between Malicefow! and Brush-tui'key

(see Tuble 8 and Fig, 4),

Tarsometatarsus

The articular impression of the Ist meta-

tarsal is prominent in megapodes and jncon-

spicuous In Gaura. The shaft is narrow below

the impression in Goura and broad in mega-

podes. The hypotarsus is more slender and

finely formed in Goura than in megapodes, The

larsometatarsi of the species of megapodes

differ in size (sec Table 9 and Fig, 4).

Relative bone lengths

In Table 10, the lengths of the limb bones

ate €xpressed in terms of coracoid Jengths.

Gonra differs by having relatively shorter

humeri, femnora and tibiotarsi, than mega-

podes, The tarsometatarsi of Goura, P. nara-

coortersts and L. ovellata are relatively shorter

than these of P. gallinacea, A, latharmi, M.

reinwardt and M. prirchardi.

219

TABLE 3

Mitasuremeniy of Humeri of Megapodes and

Crowned Pigeons

= =

EiEs =:

ue th Ro@ E = 2B

FH rs < £5 aa

3 = > » & By S28

2 Ei § = § S82 Be BE

2) Zz 2 @ 8 af &s AE

P. uuracvortensis. SAM, Pi7153 1444 36 #14 «#3

SAM, PI7154 32

SAM, P18183 49 14 «FZ

SAM, F17878—* li 26

G, victoria NMV, W6676 WS 34 «12 «25

GC. scheepmakerl NMV, RS054

ROAM AP AMA TAP AP Re eRe

L, ectilata SAM, Bllda2 io 62200~«&a

& 19

SAM, 18039 2 24 #9 19

103 24 BOY

NMY, B9276 wy oa 9 19

18 2 9 20

Aw tuthumt MMV, W964 7 21 G 18

$6 20 8

NMV, W4sS4 2 u 18

x Bs & oI

NMY, W4545 $8 oa 4 on

89 1 B. 1B

M. roinwardt CSIRO,

GALS 2 f kL @2 19 is

R HZ 19 R #616

Csi,

GALS 3 FS & 8B W a WT

R 84 19 8 16

M. orltehardi USNM, 119634 L sg 42 4 ii

R 59 12 464

* Juvenile,

Weights

Weights of seven male Mallecfowl ranged

from 2.0 to 2.2 kg and of four females from

1.5 to 1,9 kg. Weights of five male Scrubfowl

ranged from 0.8 to 1.2 kg and of seven females

from 0.6 to 1.1 kg. Maschlanka (1972) found

no significant sexual differences in the bone

lengths of Malleefowl and Sutter (1965)

Jound that of three Brush-turkcy raised in cap-

tivity, two females reached weights of 2.0 and

2.1 kg and a male 2.5 kg. This limited evidence

suggests that male megapodes are only slightly

Jarger than females.

If if is assumed that weight is proportional

to the cube of the length of the coracoid and

that the average weight of Malleefowl is twa

Fig, 3, a—tleft humerus, M. reinward? (CSIRO, GALS3): 4.—left humetus, P. naracoariensis (SAM,

P17153); c—left radius, P.

naracoortensis (SAM, P18184); ¢@—left radius, M. reinwardt

(CSIRO, GALS3); e—tleft reversed ulna. P.

naracoortensis (SAM, P17879); f—rieht ulna,

juvenile P. naracoortensis (SAM, P17877): 2— right ulna, M, reinwardt (CSTRO, GALS3): hi.

and i—right ulna, P. gallinacea (AM, F54721 and F54722).

220

TABLE 4

Measurements of Ulnae of Megapudes ana

Crowned Pigéons

UU U EEE ESSE

2 4

guf2 2

g z 2 2 Es ia ca

ia = ay 26 S Se

P. callinaceaz QM,.15553 R Hi 20

AM, F54721 R 23

AM, F54722 R 12 22

AM, F54723 R We 22

P. naracgor(ensis SAM, P17879 L ig 19

SAM, PI8182 L WwW 19

SAM, PL7877—— R 137 9 10

‘G. Victoria NM¥, W676 L it 19 9 17

R bal 18 17

G. scheepmakeri NMV, R&054 L ws 18 & 14

R 124 #17 q i4

LL. ocelluta SAM. 111482 d Tr. 105 14 % 79

R103 14 7 13

SAM. B39 OL 1068 1H AB

R 106 15 4 13

NMV, 09276 L olt:t 14 7 12

R it4 15 7 13

A, lathami NMY, W964 L RY 5 7 12

R 8 13 & IL

NMY, W4554 L #8 13 vy oat

R RE 3 7 VW

NMYV, W4555 {, AR VW 7 it

R 88 13 6 41

M. reinwardt CSIRO,

GALS 2 gf Lk 8 12 6 10

Rh 85 6 1

CSTRO-

GALS 3 4 L 87 13 5 6

R RB i3 6 1)

M. pritchard? USNM, 3.19634 r 67 & 4 7

R 66 8 3 7

—_

* Juvenile.

kg and of Scrubfowl one kg, then the weight

of P. gallinacea would have been aboul five to

seven kg and of P. naracoortensts about sour

io five kg.

A reconstruction of the relative sizes of the

Australian megapodes is given in Fig. 5.

Power of flight

There are several kinds of birds thal are

over seven ky in weight and are capable of

flying, e.g. turkeys, bustards, cranes and

swans. The wing bones of the two Progura

species are relatively and absolutely long and

slrong enough for them to have been capable

of at least Jimited flight.

Ecolagy

Until more material, especially of the skull,

of the species of Progura becomes available

for study, very little can be suid about how

and in what habitats they lived. As Jarge land

G. F. vaw TETS

TABLE 5

Measuremenis. of Radii of Megapodes ard

Crowned Pigeons

EE - 2

g 3 a

¥ EI « 3 2 £2 Ge &

a 2 &@ 2 4 & &2 aE

P. qaracoortensls SAM, PIS184 L 135 10 G 13

G. victoria NMY. Waé676 E 4720 Y) 5 1

R 120 10 5 Ww

G, scheopmakeri NMV, RB054 L ii4 7 5 10

R114 % 5 a

L, ocellata NMV, 89276 1 104 7 4 8

rR 105 7 4 §

A, lathamni NMY, WS964 L 80 3 3 K

R 79 bh 3 8

NMY, W4554 I. §1 i J 8

RK 80 t a &

NMY, W455 | Ae <2 a 4 #

R BI i) 3 ¥

M. reluwardl CSIRO,

GALS2 Jd L 7 6 3 8

R 79 6 &

CSIRO,

GALS 4 a L £0 4 3 7

kK ‘80 f 3 7

M, pritehardl USNM, 319634 L 61 § z Ss

R 5 4 2 x

TABLE 6

Measurements of Carpometacarpit of Megapodes and

Crowned Pigeons

= #

olf 2 2

3 Fi a 25 2 2

2 a = #5 <f =I

o € of 25 “ =

z = 33 5 €S SE BE

a Zz Gf a m2 FE OE

ne vue .

p.yalinacea OEM] go 27x16 IT 19

QM, FI39 4

OM, P7005, RK x16 11x94

G. victoria NMY, W676 L 6 2x12 7Txs

R 69 22x13 7x V2

G, scheepoakerd NMV, R8O54 L 64 21x11) 7x35 J4

R 65 19x12 7x5 14

L. acellafa SAM, HV14x2 a L SY (Sx 9 6x4 9

kh 54 19x 9 GeS ¥Y

NMY, 19276 L 56 Wx10 65 I

R 55 16x10 fri OB

NMY, B9037 I, 54 i548 9 Sx4 1.

R 4 Gx 9 Sa4 10

Ay lathanl NMY. WS964 L 49 3% 9 5x4 10

R 49 (2x 8 Sea 9

NMY, W454 L 47 lax 8 Sx 9G

R 47 13% 8 Sez 9

NMV, W4555 L 46 13x 8 x3 9

R 46 idx 7 Sx3 Y

M. reinwardl CSIRO,

GALS2 ak 45 j2e 7 Sx4 8

R 46 f2" 7 Sx4 &

csma,

GALS3 Gl 47 tax 7 5x*¥3 #8

R 46 Sx4 §&

M. pritchardi USNM, 319634 «=L 33 7x 4 3x2 §S

R 33 8x 4 Gx2 5

REVISION OF FOSSIL MEGAPODIIDAE (AVES)

2cm

Fig. 4. ¢,—tight tarsomelatarsus, P. naracoortensis (SAM, P17856); b.—rtight tarsometatarsus. M.

reinwardt (CSIRO, GALS3): c.—left reversed tarsometatarsus, P. vallinacva (QM, F1143); @.

and ¢.—right tarsometatarsi, P. gallinacea (QM, F5556 and F5557); f.—right femur, P. nare-

coortensis (SAM, P17857); ¢—right femur, M. reinwardt (CSIRO, GALS3); A.—right tibio-

tarsus, M. reinwardt (CSIRO, GALS3): j—tright tibiotarsus, P. naracaortensis (SAM,

PI7152); j—synsacrum, P. naracoortensis (SAM, P18187); k.—synsacrum, M. reinwardt

CSIRO, GALS3).

G. F. vaw TETS

Progura gallinacea oe

Fig. 5. Extant and reconstructed fossil megapodes of Australia.

birds, they presumably could survive in a wide

range of habitats.

The relatively long legs of P. gallinacea, the

Brush-turkey and the Scrubfowl suggest that

P. gallinucea was also a tain forest species.

Conversely the relatively short legs of P. nara-

coorrensis suggest that it was an open shrub

land bird like the Malleefowl. This assumption

is supported by the discovery of remains of

both of these latter species at Victoria Cave

together with remains of other birds of open

habitats (van Tets & Smith 1974),

Why the species of Progura died out may

be related to the extinction of many other

large vertebrates during the last peak in world

glaciation. It may have been caused hy en-

vironmenial changes in Australia associated

with increasing aridity, and with the displace-

ment of native marsupial predators by men and

dogs.

Systemutics

The matetial of Pregura indicates that there

were two very large spceics of megapodes in

south-eastern Australia, P, gallinaeeu and P-.

naracnartensis, during Pleistocene times. Other

than size there are mo clear characters that

Separate Progura from the other genera of

megapodes hor that indicate to which of these

genera it is closest. Relative tarsometatarsal

Jengths do indicate similarities belween P,

naracaorrensis and Leipoa and between P,

gallinucea and the other two Australian mega-

pode genera, Aleciura and Megapadius. Until

further fossil material becomes available for

stady and there is a modern revision of the

mainly monotypic megapode genera, it is

preferable ia use the genus Progura for the

two fossil megapode species. gallinucea and

naracoortensin.

REVISION OF FOSSIL MEGAPODIIDAE (AVES)

TABLE 7

Measurements of Femora of Megapodes and

Crowned Pigeons

223

TABLE 8

Measurements of Tibivtarsi of Megapodes and

Crowned Pigeons

en] = = =

EB g a 2 Eggs 5

ae 5 fo e3 5

: i gas? 5 3 g sf22 4

Fy E x 4 4 2 Be Be 2 E x § & $2 gs he

a Zz @ #@ 3 £2 GE AS & Zz a@ @ J &2 G6 BE

P. naracoortcusis SAM, PL7857 R 30 P. naracoariensis SAM, P17152 R 158 25 11 23

SAM, PI8!86 R 28 SAM, PL7B876 R 10 «2

G. victoria NMY, W676 L 8 1 8 19 G, victoria NMY, W6676 L 135 «#19 7 16

R88 5 19 R 135 20 7 16

G. scheepmakeri NMV, R8054 Lb 83 #49 8 18 G, scheepmakeri NMY, R8054 1, 126 17 7 14

R 83 19 8 18 R 126 18 § 14

L, ocellata SAM, BI 14B2 a L 84 «20 & 19 L. oceata SAM, B1i482 a L 121 24 G 4

R 8&4 21 8 19 R i231 25 6 14

SAM, B5039 9 TI & 20 § 19 SAM, H5039 Q L 123 22 6 3

R 64 2) 9 19 R 23 23 6 13

NMYV., B9276 L s&s& 2 g 19 NMV, B9276 L 1300 = «(21 7 1s

R S90 20 8 19. R 129 QL vi 1s

A. Jathoml NMY, W5964 L 4 21 9 #19 A. lothami NMY, W5964 L 129 «20 8 14

R 9 2 9° 19 R130 19 7 14

NMY, W4554 CL 92 #19 9 19 NMV, W4554 L 135 19 7 i4

R 9 i9 10 19 R145 19 7 14

NMY, W4555 L 0 20 W 18 NMY. W4555 L 134 ~=«18 7 14

R 89 26 9 18 R 134 18 7 #14

M, reinwardt CSIRO, M. reinwardt CSIRO.

GALS 2 a t 75 7 & GALS2 J L tld 19 7 13

R75 7 8 17 R 114 19 13

CSIRO, CSIRO,

GALS 3 J L TW 17 Tt A? GALS 3 d L 1s 20 7 13

R 77 #17 B I R 115 #19 7 I2

M, pritchardi USNM, 319634 L 52 Ww ¢ M. pritchardi USNM, 319634 L 84 12 4 g

R 42 10 4 11 R 83 13 4 8

Acknowledgments

This paper owes a great debt to the many

persons involved during the past century in

collecting, cleaning and curaling the bones

that were made available for this study by the

museums listed under methods,

I have benefitted greatly from discussions

with colleagues in these museums and jin

CSIRO. In particular I am grateful to

Jeanette Hope, Meredith Smith and Pat

Vickers Rich who brought most of the un-

described fossil megapode material to my

attention.

The figures were drawn by F. Knight.

TABLE 10

Megapode and Crowned Pigeon bone lengths

expressed as Coracoid lengths

—_—_ ee

5 5 2 43 5 £ gs

8 B 5 ¢ fe 2 2 $3

wa m= 2 e OF BR HE

P. gallinacea 1 1.6

P. naracoortensis i7 16 16 19 1A

G, victorla 1300616 465.4 OR Td L6 12

G. schvepmakort 13 26 4 O08 Ld 16 22

L, ocellata 6 1.6 16 0.9 13 19 1.2

A. lathami 1.5 1S 614° « O8 LS 2.2 1.4

M. reinwardt 1.5 6 LS O8 14 22 1.4

M. pritchardi “h6 618 #16 09 14 23 Lé

224 G. F. yaw TETS

TABLE 9

Measurements af Tarsometatarsi of Megapades and Crowned Pigeons

Shatt

width Central

below truchlea

Proximal Shaft Distal

Length width width width hallux width

Species Number Sex Side mm mm mm mm mm mm

P. galliiiacea QM, F1134 Left 29

QM, F1i43 Left 29 12

QM, F5556 Right 148 VW 13 12

QM, F5557 Right 30 11

QM, #7033 Right 10+

AM, F54724 Left 26

AM, F54725 Left 27 13 1

AM, F54726 Right 29 12 10

P. naracoorlensis SAM, P17856 Right 96 22 9 11 9

QM. F2769 Left 23

SAM, P18185 Right 21 10

G. victoria NMV, W6676 Left 98 17 7 \7 7 6

Right 99 17 7 17 7 6

G. scheepmakeri NMY, R&054 Left 93 17 ¥ i4 7 4

Right 93 17 6 14 7 6

L.. ocellate SAM, Bi 1482 Left 72 15 7 18

Right 72 14 7 17

SAM, B5039 e Right 77 16 7 17 10 6

NMY, B9276 Left 74 15 7 17 9 6

Right 74 16 7 17 y 6

A. lathami NMV,.W5964 Lett 87 16 6 16 8 6

Right 87 16 7 16 8 6

NMV, W4554 Left 89 15 6 14 8 7

Right 89 «15 6 IS 8 6

NMV, W4555 Lett 895 15 6 16 8 6

Right 90 15 6 17 8 6

M. Reinwaredt CSIRO, GALS 2 Left 76 14 6 15 7 6

Right 76 14 6 14 7 5

CSIRO, GALS 3 left 77 14 6 15 7 6

Right 77 14 4 15 7 6

M. pritchareli USNM, 319634 Left g 4 11 5 4

Right 49 9 4 10 5 4

References

Bropgors, P. (1964)-—Catulogue of fossil birds:

Part ‘2. Bull, Florida State Mus. 8(3), 195-

335,

De Vis, C. W. (18883).—Australian ancestry of

the crowned pigeon of New Guinea. Proc. R.

Suv, Qld 5, 127-131, Plate V1.

De Vis, C, W. (1888b).—A glimpse of ihe Pusl-

Tertiary avifanna of Queensland. Proc. Linn.

Sec. NUS.W. (Ser, 2) 3, 1,277-1,292, Plate

XXXY,

Dr Vis, C. W. (1889),—Additions to ihe list of

fossil birds. Proc. R. Soc, Qld 6, 55-58, Plate

TV.

De Vis. C. W. (1891).—Residue of the extinct

birds of Qneensland as yet detected, Prac.

Linn. Soc, NSM‘, (Ser. 2) 6, 437-456, Plate

XXIV.

Frith, H. J, (1962),—“The Mallee-Fowl.” (Angus

& Robertson; Sydney.)

Harvey. E. B,. Kaiser, H. E.. & RosenBerc,

L. F. (1968).—“An atlas of the Domestic

‘Torkey (Meleagris gallopavo) myology and

osteology,” (U.S, Atomic Energy Commission

Div. Biol & Med,)

Lonoman, H. A. (1945).—Fossil vertebrates from

Gore Quarries. Mem. Old Mus. 12, 164.

T.yoeKKer, R. (1891).—“Catalogue of the fossil

birds in the Brifish Museum Natural TTis-

tory.” (London. )

MASCHLANKA, Hildegard (1972).—Proporiion-

anulyse von Hihnervégeln. Z, wiss. Zoal.,

Leipzig 183(3/4), 206-252.

Scancetr. R, J, (1972)—Bones for the New Zea-

land archaeologist. Canterbury Muy. Bull. 4.

Scuncei, G, D. (1970). -A phenetic study of the

suborder Lari (Aves). I. Methods and results

of principal components Analyses, Systematic

Zoaalogey 19, 35-457.

Suirer, E, (1965).—Zum Wachstum der Gross-

fusshithner (Alectura und Megapodius). Orn,

Beob. 62, 43-60.

van Tets, G. F.. & Smitu, Meredith J, (1974),—

Small fossil vertebrates from Victoria Cave.

Naracoorte, South Australia, IIT. Birds

fAves). rans. R. Soc. S. Aust. 98(4),

225-227.

SMALL FOSSIL VERTEBRATES FROM VICTORIA CAVE,

NARACOORTE, SOUTH AUSTRALIA

III. BIRDS (AVES)

BY G, F, VAN TETS* AND MEREDITH J. SMITH]

Summary

VAN TETS, G. F.. & SMITH, MEREDITH J. (1974). -Small fossil vertebrates from Victoria Cave,

Naracoorte, South Australia. I. Birds (Aves). Trans. R. Soc. S. Aust. 98(4), 225-227,

30 November, 1974.

Abundant fossil remains of marsupials, rodents and birds have been found in Victoria Cave, near

Naracoorte, South Australia. The presence of certain large, extinct herbivores in the assemblage

suggests that the deposit may be of Pleistocene age. This paper reports the remains of: Dromaius

novaehollandiae, Emu; Progura naracoortensis, a giant megapode; Leipoa ocellata, Malleefowl;

Coturnix pectoralis, Stubble Quail; C. australis, Brown Quail; Turnix varia, Painted Buttonquail;

Pedionomus torquatus, Plains-wanderer; Rallus philippensis, Land Rail; Peltohyas australis,

Australian Dotterel; Tringa glareola, Wood Sandpiper; Gallinago hardwickii, Japanese Snipe;

Calidris ruficollis, Red-necked Stint; Chionis minor, Blackfaced Sheathbill; Pezoporus wallicus,

Ground Parrot; Tyto novaehollandiae, Masked Owl; Grallina cyanoleuca, Magpie-lark; and

Gymnorhina tibicen, Australian Magpie.

The Sheathbill is a new record for Australasia. Progura naracoortensis is extinct. Most of the other

species are still extant in south-eastern South Australia. They suggest that at the time of deposition

Victoria Cave was surrounded by savannah woodland with substantial areas of heath, wet and dry

grasslands, and mudflats.

SMALL FOSSIL VERTEBRATES FROM VICTORIA CAVE, NARACOORTE,

SOUTH AUSTRALIA

III, BIRDS (AVES)

by G, F. vAN TeTS* and Msrenitn J, Smitay

Summary

van Ters, G, F..& Smiryu, Mexenity J, (1974),--Small fossil vertebrates from Victoria Cave,

Naracoorte, South Australia. IM, Birds (Aves). Trans. R. Soc, §, Aust, 98(4), 225-227,

30. November, 1974.

Abundant fossil remains of marsupials, rodenis and birds have been found in Victoria

Cave, nesr Naracoorte, South Australia. The presence of certain large. extinct herbivores in

the assemblage suggests that the deposit may be of Pleistocene age. This paper reperts the

remains of: Dramaius nevaehollandiae, Emu; Progura naracooriensis, 4 giant megapode;

Leipoa oceliata, Malleefowl; Coturnix pectorulis, Syubble Quail: C. australis, Brown Quail;

furnix varie, Painted Buttonqnail, Pedionomus torquatus, Plains-~wanderer; Rallus phitippensts,

Land Rail; Peltohvas australis, Australian Dotterel; Tringa glureala, Wood Sanslpiper; Gal-

linage fardwickit, Japanese Snipe: Calidris ruficollis, Red-necked Stint; Chianis minor, Black-

faced Sheathbill; Pezoporus wallicus, Ground Purrot; Tyto novaehollandiae, Masked Owl:

Grallina ¢yanoleuca, Magpic-lark; and Gyminerfina tibicen, Australian Magpie.

The Sheathbill is a new record for Australasia, Prosura varacooriensis is extinct. Most of

the other species are still extant in south-eastern South Australia. They suggest that at the time

of deposition Victoria Cave wax surrounded by savannah woodland with substantial areas of

heath. wet.and dry grasslands, and mudflats.

Introduction

The fossil! bone deposits and their method

of extraction from Victoria Cave near Nara-

coorte (37°00'S, 149°48’E) have been des-

cribed by Smith (1971, 1972). They contain

remains of largé marsupials which are believed

to have become extinct at the end of the

Pleistocene (Tedford 1967), The present paper

describes bird remains that have been identi-

fied by comparison with bones of extant

species in the collections of the South Aus-

tralian Museum (SAM), the National Museum

of Victoria (NMV), the American Museum

of Natural History (AMNH), and the Divi-

sion of Wildlife Research, CSIRO.

Family DROMAIIDAK

Dromuius cf. novaehollandiae (Latham, 1790),

Emu.

A synsacrum (SAM. P1650i) was identified

by Pat Vickers Rich (pers, comm.).

Family MEGAPODIIDAE

The fossil material of megapodes from Vic-

toria Cave and elsewhere is described and dis-

cussed in van Tets (19744). It included

material of Progura naracoortensis van Tets,

1974, a mant megapode (SAM, P16700);

Leipoa ocellaia Gould, 1840, a Malleefow!

(SAM, P1i6733): and one or more juvenile

megapode(s) (SAM, P16739-45). The juvenile

Meyapode material is of a species about the

same size as Mallecfowl. but indeterminable

fo genus, and species,

Fumily PHASIANIDAE

Coternix pectoralis Gould. 1837, Stubble

Quail.

The following bones were found of at Jeast

thrée birds: three crania, two right Humeri,

two tight and one Jeft carpometacarpi, two

sternal manubria, three synsacra, one left

tibiotarsus and one left tarsometatarsus

(SAM, P16701-10 and P16746—50).

* Divisian of Wildlife Research, CSIRO, P.O. Rox 84, Lyneham. A.C.T. 2602.

+ P.O. Box 62, Magill, S. Ausl, 5072,

226

Coturnix australis

Quail.

The following bones were found of at least

four birds; ane crantum, one sight carpu-

melacatpus and four synsacta (SAM,

P}o711-6). Another synsacral fragment

(SAM. P16717) could have belonged io

either Corurnix species.

Family TURNICIDAE

Turnix sp., a buttonqiail.

One right humerus (SAM, P!6751) of an

unknown species of Turnix, which ts

neither 7. maculosa, T. varia, T. melano-

vaster, T. velox nor T. pyrrhothorax.

Turnix varia (Latham. 180)), Painted Button-

quail.

One right humérus (SAM, P16752)-

Family PEDIONOMIDAE

Pedionomus torquatus Gould, [84,

wanderer.

One synsaccum (SAM, P16718)-

Family RALLIDAE

Rallus philippensis Linnaeus. 1766, Land Raul.

One synsactum (SAM, P16719).

(Latham, 1801), Brown

Pisits-

Family CHARADRIIDAE

Peltohyas australis (Gould, 1840). Australiitn

Dotterel.

Three synsacra (SAM, P16720-2).

Family SCOLOPACIDAK

Tringa glarevia Linnaeus, 1758, Wood Sand-

piper.

One synsacrum (SAM. P16723). A proxi-

mal part of a Jeft tibiotarsus (SAM,

P11555) was collected at Naracoorte long

before 1954, when it was registered.

Gallinago hardwickii (Gray, 1831), Japanese

Snive.

Three synsacta (SAM, P16724-6),

Calidris ruficollis (Pallas. 1776), Red-necked

Stint,

Four synsaeta (SAM, P16727-30).

Family CHIONHDAE

Chioniy: minor Harilaub, 1841.

Sheatbbill,

One synsacrum (SAM, P16731). Jt was in-

distinguishable from ‘synsacra from extant

Chionls minor ({NMYV., W2234, W3457,

W6443, Wé6dd4 and W64746) collected al

Kerguelen and Heard Islands. A synsacrum

of Chionis alba (AMNH, 879), differed

Black-faced

G. F. van VETS & MEREDITH J, SMITH

mainly by having an additional vertebra

fused to the anterior end.

Sheathbills have not previously been re-

ported in Australia. They now only occur in

sub-antarctic regions, Chionis alba around the

tip of South America and Ch, minor on islands

svuth of the Indian Ocean. They scavenge on

beaches and icebergs. It is possible that some

rafted ta Australia during a glicial period and

diced out during the subsequent inter-glaciut

petiod, There is no evidence of sheathbills hav--

ing ocurred at Macquarie Island and at the

sub-untuarctic islands of New Zenaland. where

there should be suitable habitat tor them.

Fumily PLATYCERCIDAE

Pezoporus wallicus (Kerr, 1792),

Parrot,

Three naso-premaxillac (SAM, P16732-4).

Ground Parrots occurred in the Naracoorte

area in historic times, but are now Jacally

extinct becuuse of habitat destruction.

Family TYTONIDAE

Tyto novachollandiae (Stephens.

Masked Owl.

Cranium (SAM, P16735) and a synsacrum

(SAM, P16736)

Family GRALLINIDAE

Grallina cyanoleuca (Latham, 1801), Magpie-

lark,

One synsacrum and a distal part of a left

tarsometatursus. (SAM, P16753 9 and

P16754).

Family CRATICIDAE

Gymnorhina tibicen (Latham, 1801), Austra-

lin Magpic.

One Jelt humerus (SAM, P16737). Two

forms of Gyatiorhina may occur in the

Nardcoorte urea, tibieen and Aypoleuca.

They are considered conspecific hy some

and sepurate species by others.

Graund

1826),

Discussion

ta) Method of acceumuluien of deposit

Because of the preponderance of juvenile

remains among the larger mammal species as

compared with a greater proportion of adults

among the smaller specics, Smith (1971,

1972) postulated that the small vertebrate re-

mains were brought to the cave by predators,

‘The bird remains are not inconsistent with

this. hypothesis, bul are too few to support

iv.

FOSSIL BIRDS FROM YICTORTA CAVE. NARACOORTE 227

Remains were found of an avian predator,

the Masked Owl and an avian scavenger, the

Black-faced Sheathbill, The owl is known ja

have inhabited caves.on the Nullarbor Plain ot

South Australia (Richards 1971) and is able

lo prey on animals up to the size of small

rabbits {Calaby 1969). The sheathbill also

nests im caves and crevices (Downes. ef al.

1959}, On the Nullarbor Plain, the Peregrine

Falcon. Falca peregrinux, Brown Fulvon, F.

berigord, and Nankeen Kesirel, F. cenchraides

reside in cave entrances (Richards 1971). Re-

mains of the Brown Goshawk, Accipiter fuscia-

tus were found in Weekes Cave on the Nullar-

hor Plain (van Tets 1974b).

Some of the bird remains could have come

Fram ow! pellets or from carcasses brought ito

the cuve by avian and mammalian predators

und scavengers, Another explanation may have

to be found for the great number of synsacra

with Mo associated bones. They are of small

wetland hirds in the families Pedionomidae,

Rallidae, Chiradriidae and Scolopacidae, ‘The

remains of these birds may have been washed

into the cave and the synsacra may have been

separated from the other bones by the wash-

ing and sorting action of running water,

(b) Climarie interpretations

From the small mammal remains, Smith

(1971. 1972) concluded that at the time of

deposition Victoria Cave was surrounded by

sclerophyll forest,

The bird remains. suggest the presence of

savannah woodland with substantial areas of

heath, wet and dry grassland and mudfiats.

All the bird species found thrive under wet

coastal conditions, although some of them also

occur in dry inland locations. Except for the

extinct giant megapode and the sheathbill, al)

the bird species found have occurred in south-

eastern South Australia in historic times (Con-

don 1968),

Acknowledgments

Excavation of the deposit would not have

proceeded without the enthusiastic help of

CEGSA members in digging and sieving.

Transport costs for these helpers were defrayed

hy a grant from the South Australian Govern-

ment Tourist Bureatt. The late Mr, B. Mad-

dock ably mediated between CEGSA and the

Tourist Bureau and actively assisted in the

working of the deposit.

We are grateful for the advice and help we

received during the examination of the avian

material from: Dr Pat Vickers Rich

(A.M.N.H.); Mr. A, R. McEwey (N.M.YV.):

Mr. H. T. Condon and Mr. N, Pledge

(S.A.M.}; and Mr. J. H. Calaby, Dr, R.

Schodde and Mr. FE, Slater (CSIRO).

References

Catasy, J. H, (1989) —ae H. J, Frith, ed. “Birds

in, the Australian Tigh Country’, (A. H.

& A.W. Reed: Sydney.)

Convon, H. T. (1968).—"A handlist of the birds

of South Australia” Ind Bd, (S:A-OLA,: Ade-

lade.)

Downes, M, C., Eauey, B, A. M.. Gwyen, A. M.,

& Youne, P. §. (1959)—The birds of Heard

Island. ANARE Reports Series B Val {

Zoolory, 1-135,

Rictiarps, Aola M, (1971)—An ecological study

of the cavernicolous fauna of the Nullarbor

Plain, southern Australia, J. Zeal. wort,

164, 1-60.

Smith, Meredith J. (1971)—Small fossil verte-

brates from Victoria Cave, Naracoorte. South

Australia. 1. Potoromae {Macropodidae),

Petauridae and Burramyidae (Marsupinlia).

Frans. R. Soc. S. Aust 98(4), 185-198,

Smita, Meredith J. (1972)—Small fossil verte-

brates from Victoria Cave, Naracuorie.

South Australia, 1, Peramelidae. Thvlacini-

dae und Dasyuridae (Marsupialia). Trans.

RK. Soe, 8, Aust, 9643), 125-137,

Troroxp, RB, H,. (1967)—The fossil Macropo-

didue from Lake Menindee, New South

wet Univ Calif. Publ. Geel. Sei. 64, J-

156.

VAN Tks, G, TL (197da)—A revision of the

fossil Megapodiidae, including a description

of a new species of Progura De Vis. Trans,

R. Sow. 8. Ausl, 98(4), 213-224,

VAN TEIs, G. F, (1974h)—-Fossil birds (Aves)

from Weekes Cave, Nullarbor Plain. South

Australia. Trans, R, Soc, S. Angst. 98(4),

229,250.

FOSSIL BIRDS (AVES) FROM WEEKES CAVE, NULLARBOR PLAIN,

SOUTH AUSTRALIA

BY G. F. VAN TETS*

Summary

VAN TETS, G. F. (1974). -Fossil birds (Aves) from Weekes Cave, Nullarbor Plain,

South Australia. Trans. R. Soc. S. Aust. 98(4), 229-230, 30 November, 1974.

At Weekes Cave, a sink hole on the Nullarbor Plain near Koonalda Station, South Australia,

remains have been found of Platibis flavipes, Yellow-billed Spoonbill; Accipiter fasciatus,

Brown Goshawk; Falco cenchroides, Nankeen Kestrel; either Turnix velox or T. pyrrhothorax, a

buttonquail; = Cinclorhamphus cruralis, Brown Songlark; Cinclorhamphus —mathewsi,

Rufous Songlark; Poephila guttata, Zebra Finch; and Artamus leucorhynchus, Whitebreasted

Wood-swallow. Some of these birds times.

FOSSIL BIRDS (AVES) FROM WEEKES CAVE, NULLARBOR PLAIN,

SOUTH AUSTRALIA

by G. F. vAN TETS*

Summary

van Trers, G. F, (1974).—Fossil birds (Aves) from Weekes Cuvée, Nullarbor Plain, Sovth

Australia. Trans. R. Soc, 3. Aust. 98(4}, 229-230, 30 November, 1974.

At Weekes Cave, a sink hole on the Nullarbor Plain near Koonalda Station, South

Australia, remains have been found of Platihis flavipes, Yellow-billed Spoonbill; Accipiter

jasciatus, Brown Goshawk; Falco cenchroides, Nankeen Kestrel; either Turnix velox or T,

pyrrhothorax, a buttonquail; Cinelorhamphus cruralis, Browa Songlark; Cielorhamphus

mathewsi, Rufous Songlark; Poephila guttata, Zebra Finch; and Artarius leucorhynchiis, White-

breasted Wood-swallow. Some of these birds require a less arid climale than has prevailed on

the Nullarbor Plain in historic times.

Introduction

Weekes Cave (N15) is a sink hole near

Koonalda Station on the Nullarbor Plain in

South Australia, near the border with Western

Australia. Multiple entrances drop 10m to

a flat silt-floored chamber (Hill 1967). ‘The

bird bones reported in this paper were collected

by members of the Cave Exploration Group

of South Australia, and are part of the collec-

lions of the South Australian Museum (SAM).

The bones were identified by comparisons with

reference bones in the collections of the

National Museum of Victoria and the Division

of Wildlife Research, CSIRO,

Family THRESKIORNITHIDAE

Platibis flavipes. (Gould, 1938), Yellow-billed

Spoonbill,

Almost compicte skeleton (SAM, P17927)-.

Family ACCIPITRIDAE

Accipiter fasciatus Vigors & Horsfield, 1827,

Brown Goshawk.

Skull (SAM, P18060) snd a synsacrum

(SAM, P18061).

Family FALCONIDAE

Falco cenchroides Vigors & Horsfield, 1827,

Nankeen Kestrel.

Skull (SAM, P18062), This species nests

and roosts in several caves on the Nullar-

bor Plain (Richards 1971).

Family 'TURNICIDAE

Turnix sp., a buttonquail.

Four crania (SAM, P18063-6), and a right

libiotarsus (SAM, P18067) resembling Turnix

velox (Gould, 1841) and T. pyrrhothorax

(Gould, 1841), At present only T. velox oc-

curs in the area (Condon 1968. McEvey &

Middleton 1968),

Family SYLVUDAE.

Cinclorhampbus cruralis (Vigors & Horsfield,

1827), Brown Songlark.

Sternum (SAM, P1i8068). One was noted

on the Nullarbor Plain by McEvoy &

Middleton (1968).

Cinclorhamphus mathewsi

Rufous Songlark.

Skull (SAM, P18069),

Family ESTRILDIDAE

Poephila guttata (Vieillot, 1817), Zebra Finch.

Skull (SAM, P15070),

Family ARTAMIDAE

fredale, 1911,

Artamus leucorhynchus (Linnaeus, 1771),

White-breasted Wood-Swallow,

Three skulls (SAM, P18071-3).

Discussion

Some of the bird species, notably the

Yellow-billed Spoonbill and the White-breasted

Wood-swallow, require wetter conditions than

have prevailed on the Nullarbor in tecent

* Division of Wildlife Research, CSIRO, P,Q. Box 84, Lyneham, A.C.T. 2602.

230

times, As a group, the bird remains found in

the cave are those one would expect to see in

savannah woodlands with areas of open grass-

lund and shallow pools of water. They may

have come on to the Nullarbor Plain during

brief spells of exceptionally wet weather and

sought shelter in the cave when the country

dried up again.

The spoonbill may have become trapped in

the sink hole after blundering into it. Some

of the smaller birds may have been brought

into the cave by hawks and owls. Tyio novae-

hollandiae (Stephens), Masked Owl, formerly

resided in caves on the Nullarbor Plain and

G. F. van TETS

Falco peregrinus Tunstall, Peregrine Falcon,

F. berigora Vigors & Horsfield, Brown Fal-

con, and F. cenchroides, Nankeen Kestrel, still

reside in them (Hamilton-Smith 1967, Richards

1971).

Acknowledgments

I am grateful to those who collected the

bones and to Mr. N. Pledge for bringing them

io my attention. I have benefitted from dis-

cussions about the cave and ils bones with

him and with Mr. J. H, Calaby, Mr. L. Hall,

Mr, E. Hamilton-Smith and Dr. R. Schodde.

References

Cowpon, H, T. (1968).—"A handlist. of the birds

of South Australia’, 2nd Ed. (S.A.0.A.;

Adelaide).

Hamicton-SMitH, E. (1967)—Fauna of the

Nullarbor caves. /# Dunkley, J. R.. & Wig-

ley, T. M, L, (Eds.), “Caves of the Nullar-

hor”, pp. 35-42. (The Speleological Research

Council Ltd., University of Sydney.)

Hn, A. L. (1967).—Checklist of caves and re-

lated features. Ja Dunkley, J. R., & Wigley,

T. M.L. (Eds.), “Caves of the Nullarbor”,

pp. 50-61. (The Speleological Research

Council Ltd., University of Sydney.)

McEvey, A. R., & Mippteton, W, G. (1968).—

Birds und vegetation between Perth and Ade-

laide, Emu 68, 161-212.

Ricuarps, Aola M. (1971).—An ecological study

of the cavernicolous fauna of the Nullarbor

Plain, southern Australia. J. Zool, Lond.

164, 1-60.