CONTENTS

N. H. Lupsroox: Correlations of the Tertiary Rocks of Australia - -

H. H. Frntayson: The Hee OSS nessa os SA RAIO: isin, peak

Australia - -

C. H. S. Warts: Larvae of Australian Dytiscidae (Coleoptera) - -

J. N. Jennincs: Some Geomorphological Problems of the Nullarbor Plain

R. L. Specut (with J. B. CLe~anp): Flora Conservation in South Australia.

Part II. The Preservation of Species Recorded in South Australia -

D. F. Smiru: Plant Ecology of Lower Eyre Peninsula, South Australia -

J. A. Mumme: Geophysical Survey of the Officer Basin, South Australia -

R. Crawrorp: The Wooltana Volcanic Belt, South Australia - - -

H. W. Fanver: The Wooltana Lavas - - - - - - -

G. R. Heatu: Stonyfell Quartzite: pes Sree cee ee

graphy of the Type Section - -

Kinestey J. Mitts: Structural Geology of the Mt. Crawford Granite Gneiss

and Adjacent Metasediments - - - - - - - -

J. L. Tasor: eae RAEtADaCup Sc of the Bese sa COBB South

Australia - - - - - -

J. A. MummeE: Crustal Thickness in the Maralinga Area, South Australia -

R. Orrver: Structural Ecolvey of the Strathalbyn Anticline, nee

Australia - - - : : : 2 2 :

R. Scuoppe: Taxonomic Revision of the Genus Millotia Cassini - =

S. J. Epmonps: Two New Echiuroids (Echiuroidea) from Australia - -

Obituaries:

Herbert Womersley, A.L.S., F.R.E.S. - - - - - - -

Charles Mervyn Deland, M.B., B.S., D.P.H., D.T.M. - - ce ph;

Herbert Mathew Hale, O.B.E. - : . : 4 !

List of Lectures and Exhibits - - - : E : 2 a

Balance Sheet - - - = - : : : : = s

Award of Verco Medal - - : E : : 4 E 4 -

Amended List of Fellows - : 2 * E 2 = . -

New Species and Varieties Described in this Volume - - - -

123

155

159

167

185

197

199

209

243

249

253

254

255

256

257

263

CORRELATION OF THE TERTIARY ROCKS OF SOUTH AUSTRALIA*

BY N. H. LUDBROOK

Summary

Marine and non-marine sediments of Paleocene to Pliocene age are represented in South Australia,

although parts of the sequence are known only from subsurface sections. The Tertiary sequence is

most complete in the Murray Basin, where Hantkenina alabamensis compressa occurs near the top

of the Eocene and the evolutionary series Globigerinoides triloba-Orbulina universa occurs in the

Miocene. Three members with distinctive molluscan faunas occur in the so-called Pliocene of the

Adelaide Plains Basin. Charts are given showing the sequence of key foraminiferal faunas

throughout the Tertiary and of the vertical distribution of mollusca in the “Pliocene” sediments west

of Adelaide. A table is given showing the correlation of nil known formations of Tertiary age.

CORRELATION OF TILE TERTIARY ROCKS OF SOUTIT AUSTRALIA’

by N. H. Liansrookt

[Read 12 July 1962]

SUMMARY

Marine and non-marine sediments of Paleogene to Pliocene: ave are repre-

sented jo South Australia, altlough parts ef the sequenve are known only from

subsurtice sections. The Tertiary sequence is most complete ie the Murray

Basin, where Hantkenina lebanvensis compressa vous near the top of the

Eocene and the evolutionary series Glohiverinoides trilaba-Orbulina wniversu

aceurs in the Miocene, Three ameubevs with distinctive molluseaun faunas occur

im Ui so-called Miseene of the AdWaide Mans Basin. Charts are sven showing

the sequence of key: foraminiferal faunas throughout the Tertiare and of the

vertical distribution of mnalusea in the “Plincene” sediments west of Adelaide,

A table ds given showing the correlation of all knuw1 formations of Tertiary «we,

INTRODUCTION

The vontinually inereasing volume of information which becomes available

tor paleontological research from extensive econymie exploration of South

Austria by the Department of Mines and hy private companies emphasizes

the need for rewiewiny the present state of knowledue af the ‘Tertiary sediments

which cover a large part of the State and which are of majur economic import-

unce us one of the main sources of undergrouud water.

Correlation of the Tertiary rocks of southern Australia generally passed

through many vicissitudes in the first fifty years of this century and it must be

difficult for the reader to assess (he vielidity of the ages attributed tu ‘Tertiary

sediments where no indication is given of the evidence upea which the age

is determined and where no attempts are made to appraise the data available.

‘The remoteness of Australia froin Europe increases the difficulty of dating

Tertiary strata in terms of Europeun type stages, but within the last ten to

fiftecu years micropalaeontulogists have tended to attach increasing importance

to planktoniv foraminifera as Tertiary biostratigraphic indices, Although agree-

ment is aot vet general, particularly on mid-Tertiary correlation, there are several

microfaunal datum plumes, notably in the Upper Eocene and Lower Miocene,

which can be extended over Jong distances.

When planktonic foraminifera are rare or absent, which is frequently the

case in South Australia where sedimentation in some basins took plawe with

auly partial aceess to the open sea, one must rely on benthanie foraminifern

aid other groups. The mollusea have received more attention than other

phyla, but they bave limited application in detailed subsirface correlation

where percussion drilling has been used.

® Prestilental addtoss delivered ta the Roya! Sewety af South Australia on 12th July, 1963,

{ Sentar Pulacontologist, Geological Survey of Suuth Australia; pnblshed with the per-

issn OF the Director ol Mines.

Trans. Roy. Soc. $. Aust. (1963), Vol, 87.

6 N. WH, LUDBROOK

T have attempted in Fig. 1 to draw up w correlation chart for all the Tertiary

rocks known te main South Australia.

These include uot only the normal marine sediments but also paralic and

now-marine carbonaceous sediments which have yet to be precisely correlated

from palynological data. T have also prepared a biostratigraphic column te

demonstrate the more important faunal bases upoo which the correlations have

been made. Most of tlie faunas are as yet undescribed.

Working independently, Carter (158, 1959) and Jenkins (1960) made

subdivisions of the Victorian Tertiary, mainly on the evidence of planktonic

foraninifera, Carter established ua sequence of 11 faunal units for the Kocene-

Miovene of Victoria while Jenkius proposed 1 zones for a sequence in Likes

Entrance Oil Shaft corresponding approsimately to Carters faunal units 6 to 11.

A similar succession in the Viwray Busin in South Australia has also been

identified (Ludbrook, 1961, Tables X, Xf).

On the correlation chart (Vig. 1) I have indicated the correspondence

between Carter's and Jenkins fanmul units or zones and the faunal succession

in South Australia so Far as it is known ut present.

With the exception of the drawings of foraminifera, the figures have been

prepared by Mr. M. B. Langsford and Mr, J, Darnhergs of the Department of

Mines.

PALEOQCENE

Although no outerops of Paleocene rocks are known in South Austrulia,

glanconitic sands and grits occurrmg at depths of frora 3,000 to 4,000 feet in

the Gambier Sunklands are to be correlated in part at least with the Bahgallah

Formation which unconformably overlies the Cretaceous Runnymede Formation

ut Killara Bluff eight miles sonth-sonth-west of Casterton in Western Victusia.

Ferruginization indicates that these greensands were exposed before the

overlying Dartmoor Formation was deposited. Both are included in the Knighit

Group.

LOWER TO UPPER EOCENE PARALIC SEDIMENTS

During most of the Eocene, deposition under paralie conditions took place

over much of the southern part of the State. The sediments laid dewn ure

considered to be of Middle and Upper Vocene age for the most part, but it is

likely that the Lower Rocene is also represented in some areas of deeper

sedimentation,

Most of the Lertiary lignites and carbonaceous beds occur at different levels

within this sequence. “Uhvir considerable distribution, particularly along the

margins of the major basins up against the bedrock highs or in areas of shallow

basin developments in crystalline bascanent racks has been proved by extensive

drilling programmes. None have as yet been economically exploited.

In the west of South Australia, at Maralinga lignite occurred in Bove 3B

at 220 feet and in 11B at 457 to 462 feet: the Malboorna area ‘has recently heen

drilled by the $.A. Department of Mines, but results are not yct published. At

Pidinga in the Euela Basin lignitiferous clays onterop; a 48-foot borehole proved

two lignite scams 5 ft. 9in. below 23 ft. 6 in. and 7 ft. below 34 ft. depth,

On Eyre Peninsula Eocene carboriacevus sands and silts. cecur in the Min-

nipa, Cummins, Wanilla and Lincoln Basins. In the Cummins Basin the Eocene

a lo ee ia | ah

Gum Creek Holletr Co Hallet ee ui Wallaroo Ea F ra 7 yf

ASTIAN Norwest Bend Formation hs Se i] Ses rs Fishery Bay LA

By a a

YY P? SY, VI, ; AL,

PLAISANCIAN Loxton Sands Gg

Bookpurnong Beds

a Se ifs acne Ap eee AEA ra

si Soo

TRON GZ

— LL Yay LN S WE =

Pota Limestone f 7

RA RRETALIAN Morgan Cadell Marl WL / F

Limestone /

| sNevaesorte

| jNaraecarte a

Mannum Formation

FORAMINIFERAL|2 AUSTRALIAN

ZONE STAGE

CARTER UNIT

JENKINS ZONE

? Non-marine

sediments

KALIMNAN

MIDDLE | UPPER |LOWER/UPPER

CHELTENHAMIAN

BAIRNSDALIAN

BALCOMBIAN

Orboling univerea

Porticulaaphacio

fronmforia

Glodnyerinoides

Hispheericus

G. tribola tribola

Nullarbor

Limestone

BATESFORDIAN

AQUITANIAN LONGFORDIAN

Gambier Limestone

CHATTIAN

‘ suing 2

Vas ree

JANJUKIAN

RUPELIAN

LATTORFIAN

OLIGOCENE

Blanche Point

BARTONIAN rls Inkerman Cummins JOHANNIAN

Balaklava Wanilla

cool and

sequence Lincoln Bluff

AUVERSIAN Basins Limestone

primitive

Globorotalia

cf tribulosr

Non-marine

sills

and. sands

areas River Tortachilla

Greensands Kingston ane Ly

Greensands

Ken! Tawn

ie Sauth Maslin Sonds:

Moorlands

Coal Measures

LUTETIAN Knight Group

Harnpton

Conglomerate

Pidinga

Moralinga

Knight Group Dartmoar Formation

undiflerentiatec

CUISIAN

YPRESIAN

PALEOCENE

“Trans. Roy, See S:A 7. Vol. 87. Fig.l.) Carrelition of the Tertiary rocks ob South Australia,

Lone

THANETIAN

CORRELATIONS, TERTIARY ROCKS OF AUSTRALIA 7

necirs between depths of 85 und 330 feet, with black earthy lignites between

115 und 195 feet. A few paupcrate and mostly planktonic foraminifera are

usally present also. Dark grey lignitic and pyritie sunds with Clobizeriru,

Chura aud pyritized gastropods are present below 62 feet in the Wantlla Basin.

Similar sediments occur in the Lincoln Basin.

in the St. Vincent Basin the North Maslin Sands at the base of the Tertiary

sequence are of considerable economic importance. They were deserihed hy

Reynolds (1953) from Maslin Bay anc. are being extensively exploited in the

vieinity of Maslin Bay for building sands. They are uncoutormubly overlain

by the South Maslin Sands from which R. Brown of the University of Adelaide

collected a small fauna of rare mollison containing Proaneula tetet (Finlay),

Clycymeris lenticularis (Tate), Arca equidens ‘Tate, Glans curte (Tate), cf.

Alitra varicusa Tate, and species of Bimaryginula, Turhonitla, Cerithtella and

Amphilhelamus, This faund may be compared with that occurring in the ¢reen-

sands of Kent Town Bore and bores at the Children’s Hospital at depths of

wtbout 65 feut.

Low rank coul oeenrs ut intervals throughout the Laccue of the St Vincent

Basin. At Clinton 19 bores proved coal at an average depth of 292. feet with

averige Uhieckness of scam 21+8 feet, In the Inkerman-Balakliva field 34 hores

proved lignite of average thickness 18 feet at 233 feet depth. Coa! sears aeeur

on the upthraw side of the Para Fault ba the Adclaide area, At North Adelaide

they are at 111-156 fect below 80 feet of Tertiary marls and silts, Near Hope

Valley and Golden Grove 46 holes proved a small tonnage with an average aver-

burden of 150 feet. At Noarlunga nine holes proved coal at depths varying from

TO ta SIO feet die partly to disturbance anc partly to the stratigraphic position

of the seams. Coal with fossil fruits was intersected wt 80-90 feet in a water

bore in the North Maslin Sands at Kanzarilla,

Remnants of carbonaceous sediments with fossil fruits in the Barossa Vulley

and outcropping neav Lyndoch are thousht to be equivalents of the North

Maslin Sands,

Lignitic sands of presurmed Kocene age vecur in the Pirte-Torrens Basin,

while Tertiary carbonaceous sediments at present mol preeischy dated ocenr in

the Willochra Basin.

Carbouaccous sands with Eocene microflorus are known also from the Great

Artesian Basin in Lake Iyre (Ladhrook, 1963, in press) and in the Frome

Embayment.

In the Murray Basin the earliest Tertiary is represented by the Knight

Group, the formations of which for the must part are nnnamed and undifferen-

tinted Apart from those briefy deseribed (ludbrook, 196), pp, 13-14), the

Dartmoor Formation is well represented at depth in the Gambier Sunklards.

Cyclanimmina spp., Amnioadisens pirrt and fish leeth ovcor throughout most of the

sequence (“Anglesea facies") and marine intercalations with Turritella alilingae,

Ledelle leplorhyncha and corals over irregularly. The foraminifera of this

assemblage, however, are facies indicators for the most part ind do not cither

give any ¢lirect indication of the age of the sediments in which they were

deposited or permit correlation oVer more than a limited area, Fowever, they

underlie sediments with Clobuquadrina primitica and Globorvtalia ef. tribulosa

wnt are therefore of Lower to Middle Eocene age.

‘Lhe Moorlands Coal Measures and other lignitic deposits in the Uundred

of Bower, Hundred of Anna, and in County Grey oceur within and probably

lowards the top of the Knight Group.

§ N. H. LUDBROOK

All the eurly Tertiary sediments are characterized by an abundance of

Nothofazus pollen of a type occuring now only in New Guinea and New

Caledonia, The extinetion of Noethofagus is a matter needing urgent investi-

gation for the dating of non-anarine Tertiary sands and silts. Other plant

remains which have been recorded us microHforay or Fruits include the Terns

Sehizaea and Gleichenia, the comiters Podocarpuy and un Agathis similar to

Agathis palmerstoni from North Queensland, Supindaceae species close to the

Oneensland riinforest tree Misehocarpus pyrifornis, and members of Casuarina,

Muyrtacea, Banksias, Proteas, mosses,

The geographical setting tor deposition of this material was probably

similar to that of North Queensland and New Guinew today, with rainforest

bordering salt estuarics and marshes.

MIDDLE EKOCENE MARINE FACIES

The Mayurra Microfaunule

The first distinctive microfaunal assemblage in the South Australian Ter.

thiry is ain association of Globigerapsis index, Clobigerina linaperta and Clobo-

quadrine primitive which accurs in yellow limonitic quartz sand at the top of

Us Knight Group at 510 feet depth at Cellulose Australia Limited works al

Snuwzery. Hundred of Mayurra. Section 75, The same fauna ocenrs in the

lower unexposed gliuconitie member of the Wilson Bluff Limestone in the

ucla Basin where it is associated also with Kotalidtina sp., Marginulina sp.

Muaslinella chapmani and Pseudohastigerina micra (Ludbrook, L960).

The fauna occurs also at the base af the greensunds intersected at Kingston

in the Hundred of Lawepede ut 214 to 227 feet where it is assoviated with a

species of Globorotalia very close to G. ribulose Loeblich and Tappan. Globo

quadring primitiot is recorded us eecurring commonly in the Middle Bocene

but varely in the Upper Eocene in New Zealand and its known range in South

Australia sugeests that the bastr of the Wilson Bluff Limestone is of Middle

rather than Upper Eyeene age. Globorotelia ch& tribidose and its assoujited

fauna would place the base of the greensands at Kingston also in the Mickdle

Bocenc. Normal marine sedimentation continued in the Enecli Basin, but

oscillating conditions, parlicularly in the Murray Busin, tended to cause the

removal of late Kocene sediments, the correlation of which is complicated by

rupid facies cliamges.

UPPER KOCENE

(1) The Tortachille microfaminte. Globequadrina prinitiva persists in the

Wilson Blut Limestone into the next fauna which is well represented in the

upper member of the Wilson GBhalf Limestone of the Eucla Basin, the Torta-

chilla Limestone of the St. Vincent Basin. the limestone “A” ef Buccleuch Group

in the Murray Basin, wand limestone at Kingseote and Cygnet River and at depth

in the Wuadred of Menzies on Kangaroo Island.

Greensands between 120 and 214 feet depth at Kingston in the Ilnudred

ut Lacepede. greensands intersected at depths af about 60 tu 70 feet at North

Adelaide, and the Muloowurtie! Clays are to be correlated stratigraphically with

these limestones. The foraminiferal assemblage contains the planktonic species

Gslobigerapsis index and Glohigerina linaperfa nearly always accompanied by

Asterigerina adelnidensis, Maslinella chapmani, and a large Pseudopelymorphina,

1 By o typographical error, Muloawiurtic tas heen mis-spelt in Fig, 1.

PLIOCENE

LOWER UPPER

KALIMNAN

CHELTENHAMIAN | ° >

BAIRNSDALIAN

BALCOMBIAN

BATESFORDIAN

LONGFORDIAN

JANJUKIAN

OLIGOCENE

il, 4

Ayal yal

JOHANNIAN

TAHA

HHT

LOWER TO MIDDLE

“Trans. Roy. Soc. $.A.", Vol. 87.

Discorbis dimidiacus Cribrobulinina

polystoma

Peneropliy pertusus Discerbis mira

Marginopora vertebralis

Elphidium

preudonodosum

%\ Candorbulina

universa

Blorbulina

bilobata

Orbulina

universa

Porticulasphaera

—

glomerosa curva Crespinella umbonifers

Porticulasphaera

transitoria

“oe

Lepidacyclina {Tryblicleprdina)

Globigerinoides hiehnitt

Globigerinoides triloba tmmatura

bisphaericus

Austrotrillina

howehint

Globigerinaides

triloba trilobs

Globoquadrina [=

dehiscens Ye=

J Sherbornina atkinsoni

A\ Victoriella conaldea

Hofkerina s¢miornata

€24

waed,

Globigerina Guembelitria sp,

angustiumbilicata Chiloguembelina

rugosa

Mastilina torguayensis 2

Bolivinopsis crespinae

Globigerina linaperta

Hantkenina alabamensis

compressa

Maslinella chapman!

‘i

Pseudopolymorphina “SS

5P Ascerigerina

adelaidensis

Globoquadrina primitiva

Glaborotalia cf. tribulosa

Cyclammina paupera = Ammodiscus parri

Cyclammina = incisa

SA Deeparrmett of Minny

Fig, 2, South Australian Tertiary Foraminifera.

CORRELATIONS, ‘TERTIARY ROCKS OF AUSTRALIA 9

Halkyordia, Linderina, and Crespinina kingscotensis occur in the calcareous

sevliments while Sherborninw atkinsoni may be presont if the facies is saudy

(quartzose), The probable synonymy of Sherbornina atkinsoui aucl 8. eressate

lias been indicated (Ludbrook, 1961, p. 86).

Associated mollusca invariably include Turvitella aldingae and Ledello

leplorhynehia,

(2) Aone of Wantkenina alabamensis compressa, In both the 5t. Vincent

and Murray Basins the rare and diagnostic Hantkenina alaboamensis compressa

ovcurs above ov mene the lop of the unt contained in the Tortachilla and Bue-

cleuch A Jimestemes.

Tn the St, Vincent Basin it occurs, though very rarely. about three feet

thove the base af the Transitional Marl Member of the Blaache Point Marls

auc in the Murray Basin at a depth of 187-190 tee. near the top of the seqnenve

of greensands, at Kingston. These sreensands carry a similar microfauna. ta

that of the limestone of Buceleuch A and ure considered to be equivalent in

part at least te Buccleuch A. The microfauna associated with Hantkeniie

contains Globizerapsis index, Clobivertna linapertd, Astevigerina adetaidensis,

Pseudohasticerina miera, and the ostracode Cylhereis hostizea which according

tu Tornibrovk (1953, p,.38) is one of the most churacteristic iu the Upper Eocene

and Lower Oligocene of New Zealand,

This Jauma is Carter’y Faunal Unit 1.

Carter's fiunal unit 2 is probably represented by the fauna of the Banded

Vier) Member of the Blanche Point Marts, but af his tamal anit 3 is represented

iu South Australia, itapppears to be reccguizable only by Carter's criterion —the

absenee of species restricted to the Upper Kocene Units 1 and 2. Tr may

possibly be represented by the wpper park of the Bhinehy Poinl Viuwls in the

St. Vincent Basin, but isso far not identifiable above the Méntkenine zone of

the Murruy Basin, the sequence in this part of the Tertiary being governed hy

oscillation producing rapid facies change and erosion before deposition of the

Gambier Limestone. Carter (1939, p, 48+ has used the stage name Johannian

lor shila containing his urits 1, 2 and 3.

OLIGOCENE

‘The basal glauconitic member of the Gambier Limestone oceurs at depth

in the Millicent-Beachport-Kingston area and is entered at» depth of 440 teet

in borings at Cellulose Australin Ltd., Snuggery. ‘The fauna contains elements

of Carter's: Units 3 und 4, Unit 3 is represented by the persistence af Vavi-

nulinopsis acanthonucleus. Bolivinopsis crespinae and abundant Chiloguem-

belina rugosa, but Glohivgerinag laaperte is replaced by Clohigerina angustinm-

bilicata, which appears to be long-ranging (ames et al,, 1963, p55), Cuembe-

litria sp. alse occurs sparingly in tis fauna, which inchides also Gaudriina

(Pseudogaudryine) crespinae, Stomatorbinn concentrica, Vuleulina sp.. Amnio-

dlisens parri, Cyclammina paupera, C, ratundata, Vaginulinopsis. cf. gippslandieus,

wid Epistomina elegans, Victoriella cenoidéa appears immediately above this

fauna inthe Beachport area, but makes its first appearance at this level at King-

ston and Snuggary where the faynas also contain Cibicides wmbonifer and an

unornamented, probably new, species of Hofkerina. All available evidence

points. lo an Oligocene age for this unit. In Victoria it is represented by the

fier episode of the Janjukian stage (Carter's Unit 4), Tt is known so fur only

from the Murray Basin in South Australia,

10 Nh, H. LUDBROOK

The upper episode of the Janjukian is represented in the lower part of the

upper member of the Gambier Limestone with abundant Victoriella conoidea

accompanied by Hofkerine semiornata. Most of the associated globigerines are

probably G. praebulloides and G. angustiumbilicata, but Globigerina ciperoensis

is occasionally present. It makes its appearance only LO feet aboye Victoriella

conoidea in Canopus No. L Bore (Ludbrook, 1961, Table IX) and is present also

in dark grey mudstone associated with Guembelitria sp., Chiloguembelina

rugosa, Sherbornina atkinsoni, and Bolivinopsis crespinae at the top of the

Ettrick Formation in Department of Mines Bore 996/61, Hundred of Finniss,

Section 456/7, four miles east of Mannum at 5S ft. 6 in. depth, Globiverina

‘ve Maralinga

3 wenMalboor So LL,

Fhe — z>.Malboome ; 25 Leigh Cresk

; 2

Teregole

ws,

“ ti Tepe. Lake

ce Pidinga a 3 Cline

of Eocene seaimentation__— —

SCALE

MILES 50 50 190 {50 200 250 300 MILES

ee |

_ Mt Gambier age

Fig. 3. Areas of Eocene Sedimentation in South Australia,

CORRELATIONS, TERTIARY ROCKS OF AUSTRALIA 1]

ouachituensis and Globicerinw angustivorbilicata ave also present in this tuvne.

Globigerina cuapertura Jenkins oveurs al a depth of 101 to 138 fect in the same

hore ussoeiated with Sherborning atkinsoni,

The mars of the Bttrick Formation almost always contain Masyilina toi-

guayensis and Cassidulina subglobosa. Planktonic foraminifera are rare. How-

ever, the planktonics occurring in the more varied strata of the Formation in

the Moannum area confirm tut the Etirick Formation is “Janjukian”, with

fauna equivalent to Carter's Unit 5. Carter's Unit 6, Jenkins's Zone 2, with C.

ciperoensis, is represented only at the very top of the Formation,

‘The Point ‘Turton Limestone on western Yorke Peninsula also carries Vie-

toriella conoidea and is to be correlated with part of the Gambier Limestone,

althongh its fuma is very inadequately known,

The Oligocent-Miocene houndary is still a matter of some uncertainty,

Eames and his colleagues (1962, p. 21) hove presented reasons for regarding

faunul Unit 5 as lower Aquitanian, Put the strong Paleogene eloment popeseented

by Chiloguembelina rugosa, Bolivinopsis crespinae, Guembelitria sp., and Sher-

hornina atkinsoni, combined with the facts that at least alone the marging of

the Murray Basin there is discontinuity between the Bttrick and the overlying

Mannum Formations and that there is no evidence tu suggest that the Paleogene

elements could he derived, tends to support the Oligocene age attributed to the

Ettrick Formation and its equivalents (Liidbraok, 1957, 1961).

MIOCENE

The Miocene sequence in the Murray Basin has been described (Ludbrook,

1957. 1961), the Longfordian Stage being represented in the Manuum Formia-

tion, Carter's redefinition of the Longfordian (1959, p, 50) to inelnde his units

G6, 7 and & necessitates the inclusion af the Finniss Clay and the basal part of the

Morgan Limestone, which contains unit 8, within the Longfordian.

The fauna contained in the Gambier Limestone at its type locality (Lud-

brook, 1961, p. 28) with Globigerinoides rubra but without G, hisphaericus

appears to belong rather to the top of Jenkins’s Zone 4, io. below unit 8, there

beans some discrepancy between Carter's and Jenkins’s planktonic ranges at

thes level.

Equivalents of the Mannum Formation with Lomgtordian faunas are (0 he

found in the Port Willunga Beds on beth sides of Culf St. Vineent in the

Willunga and Nourlnnga Sub-basins with the type Jocality at Port Willunga

and on the eastern side of Yorke Peninsula notably at Klein Point near Stansbury.

Thev usually have abundant Sherbornina atkinsont near the base and Sher

bornina cuncimarginala and a new species of Crespinella at higher levels,

Operculina victoriensis is common except at the lower levels. The Longtortian

Stage is believed on the evidence of the planktonic foraminifera to be upprosi

mately equivalent to the European Aqtuitanian.

The Butesfordian Stage with Carter's Uuit 9, ocours wethin the Morgan

Limestune where Lepidecyclina (Trybliolepidina) howchini vcwurs in exposures

at Caloote, Mannmitn and Blanchetown. Bryozoal limestones with the sure

fauna oeour in berings at Myponga, while the Mclton Limestone exposed in

a large sinkhole two miles nerth of Mellon on Sectiin 388, Hwadred of Kulpara,

is rich in Lepldoeyelina hewchini alsv,

Limestones occurring at and to the north of Wallaroo are not yet studied

in detail and their correlation is uncertain.

12 \. Tf, LUDBROOK

The upper part of the Morgan Limestone and the Jower part of the

Pata Limestone, in which the evolutionary series leading to Biorbulina bilolata

and Orbylina. wrtiversa occur (Ladhrack, 1961. pp. 88-89), contain Jenkins’s

Zones 6 wn 9 and Carter's faunal units 10 and 11, whieh, acearding to Carter

(1959, p. 50) oecur in the Balcombian and Bairnsdalian respectively.

This sequence, according to Eames. et uf, (p. 28) bas been dated as Bur-

divulian (and/or Aqunitanian),

The position of the Nullarbor Limestorw of the Eucle Basin is a little

uncertain as the famas have not beew adeqmately studied. Most of the pulacon-

tological cata are contained in unpublished reports (Ludbrook, 1954a, LY54b,

1156, 1959b, 1959c) of the Department of Mines, which are available for

reference,

The base of the Nidlarbor Linestone measured at the Head of the Bight

(Ludbrook in Claessner and Parkin. 1955, p. 133) and also at Madura in

Western Anstralia, is correlated with the upper part of the Mannum Formation

and is probably uppermost Longtordim (Aquitanian) particularly oan the

western and northern mergins of the Enela Basin. Austrorrillina homwechini

oceurs commonly du the dense miliolid limestone frequently in association with

Flosculinela bontangensis and Maratneporn wertebralis (Ludbrook. 1954a, b).

This part ot the Nullarbor Limestone has been correlated (Ladbrouk, 1954a:

Cresomo, 1956) with the Trealla Limestone of Western Australia and ts romurnded

us Burdiglian.

The molhiscun fauna of the limestone quarried at Watsor and also at

Naretha in Western Austrulin contains such clements as MilHin sp. and Diastorna

which are usually present only ia the late Mincene or Pliocene. So fur dhe

Austrotrillind howehial-Plosculinella bontangensis association hag heen seen only

in material from Narethas,

Dating of Etadumma Formation (Stirton, Tedford and Miller, 1961, pp. 31,

51-33, 56-57) can be only approximate until the microfloral sequence in Scuth

Australian Tertiary deposits is stadicd in detail. At present it is thoneht to be

post-Oligocene frouy tentative dating by B. E. Balme of carbonaceous sediments

whieh have been lateritized and which underlie the Etadunna Formation iy

Like Eyre (Balme, 1963, in press). 1 have elsewhere (Ludbrook. 1963, in

press) suygested that the Etadmuna is possibly not older than Miocene. The

dolomitic nature of sediments at Maralinga which may be equivalent to the

Mtudunna Formation makes it possible that these were deposited iu lagoons

miuncinal to the Lower Miovene seas in which the Nullarbor Limestone was

deposited,

PMIOCENE-PLIOCENT

Tok Posroox of Tar Boowrenxosc Brps

In the Murray Basin an uncontunmity or disconfourmity veeurs between the

top of the Pata Limestone and the Bookpurnong Beds, and the Bookpurnony

Beds are nut at all to be located ia the positiow where they have been placed

hy Fames et ad. (1962, Pig. 4), As has been pointed out (Ladbrook, 1961, p. 89)

the Bookpurnong Beds are richly glauconitie and give evidence of a marked

change in sedimentation, The base of the Bookpurnong Beds at the type

exposure at Loxton (Ludhrook. T961, p. 65) aud alsu in the standard subsurface

section (ibie., pp. 68, 70-71) contain Miocene elements, To whut extent these

have been derived in the subsurface section it is impossible to suv but in the

exposed section on Section UL, Wundred of Pyap, Operculina victoriensis is

DEPTH BELOW SEA LEVEL |FEET]

Nucula(Ennucula)kalimnoe

Nuculolennuculajvenusta

Nuculana(Scage eda} neode

NuUculana[Scacoleda) verconis

Nuculana sp

Arca negolg —

porbars cf, simulans

arbatia(Acar)coma

Cucullate corlognsis OO

Limopsis cf beaumariensis 1

Limopsis ¢ucosmus

Lissarca rubricata

Glycymerts(Tucttona) convex

Glycymaris(Tucetilla) tenu|costata

Pinelada crassicardio

Ostreo orenicela

Chiomys antiaustalis

Chiomys (Mesopeplum) incerta

Spondylus spondyloiaes ~

Myadora corrugals

eidolnaerus adelaidensis -

Eucrassatella kingicolaides

und aporema —

rdita compta

190 200 210 220 230 240 250 260 270 280

S.A DEPT OF MINES

IS BORES WEST OF ADELAIDE

cabomivpssnsd sabe

Pleuromeris Iigenollg

rel ba

Sporte a lu

Myr lea uloides -

anitiiora idonea

: , > _4|

Yow eeesPecwensPoucsee paamisgese ows)

Eomilt 9 (Gibbalucina} conf ir mans

Unga (Bellucina) nuciformls

Ca jucing belcombica

Ganimyrtea salisburyensis -

Gonimyrtea yolidior

Gonimyrtea nolabilior

Milfha hora

Paalpcing cumingi

janfacuta sericea-

antigona cognala-

Towera pernitida

Tawera incurvilamellata

Chioneryx dennanti————

Placamen subroborata —

Timaciea (Veremolpa) protomarica =>

Macoma ralphi ———

Telling albineliaides

Psuedarcopagia detrita —

actra(Electromactro) howchiniana ———

laphoromactra 5B —_—

Angpella varjabylls

Zenatiopsis an

Corbula ephamilia —

Corbula adelaidensie ——

Hate! ia angasi ~_

entalium latesuicotum

Dentalium’ yiderifalium) jaraicrescens

Dentalium(Fissidentalium) mawson)

DentaliumlAntalis) denofatum

Cadulus (Dischides) yatalensis -

Emarginula didachica

Cantharidella ocellina -

Calliostomo (Laetifauter) sp

Astele (Pulchrastele) planiconicum '

Cantharidus (Phasianotrochus)laxegemmatus —

Cantharidus (Phasianotrochus) subsimplex ‘

Leiopyrga ontena ———

Bankivi fascrata ——

Thalotia (Calfhatotia) Fictlis-— — +

Clanculus (Eur iclancu jus) eucarinalus

ganda twine ia) perglobosa —-

Isanda(Minolia) $1 ai

Spectamen planicarinatum

Spectamen prascursor ~

Teinostoma depressuium

Starkeyna pulcherrima

Astrada (pellasiraen) hesperus

Phasianello sp,

Pellax jejuna

Phenacolepas tela

Aman'thaiamus Pisi00a subDicolor

Amplitholamus(Pisinna) chrysalidus ——

Turboslia pragnovarensis ——— -—

Turbosila etimattae—

Kournella denotata ——

Poeudoliatia angas) ———

Rissiona elegantula

Diastoma provisi —-

Turri fella (Gazameda) acricula adelaidensis

Turrite|la(Gazamada) subacricula

Turritello(Gazameda) jredale! —

Tenagodus australis — ————

lcuncula 4 — -

Borilgra| sacumantus) diemencnsis ~

stata

rillaria | Zeacumantus) biyoricata —

Batiliaria(Batillarjelia) estuarina

a@nulona lirasuturalls -————

delacerit ium merultum

Bittium (Eub! {hand lawl annum —

Alttlum (Sem) bittium) subgranarium

fhertcium (Chavanicerithinm adelaidense ———

Hypotrochus penefricinctu

Hypotrochus semiplicatus "

Triphora(isoiriphora) salisburyensis — ——

AmagalAmaea) Triplicata —

Melane\ia(Morgingulima) longiconica

Syrnola(Syrnola) tincta ——

SyrnolalAgatha von siang

Turboni|la(Chemnifzia) wurongos

Purponitia Chemnitzio wisn jensis

urbonilia|Chemnitzia) Widningae

urbonilla Py’ olampros) vixcdstata

Hipponix (Sabia) conica ~

Colyptrae (Siqapatella) crassa

repldula (Zeacrypta) immersa

ylospira coronata marwicki

dlinices (Conuber) subvarians

Polinices (Canuber) balteatella

oniella weymouthensis

uatrocochlis substolida

asmatic modestind

Hesoplex (Uurexsul) suboctogonus

Bedeva crassiplicata ~~

Mitrella {Bent reno lincolnensis

Mitrella (Dentimitretia) muscula ——

Mifretia (Ademitrelia) insolentior

Phos gregsoni ——

Hinia (Reticunassa) subtopiosa

290 300 310 320 330 3

x—- —|— — ) —— |—

Tet “ts {

RarevdveveXpeecccebaccee

eet

eeeeatese eee ens nae oo

ale | — et

- rng —|——

Fusinus dictyotis —

Tavoniotha Tasmanica ————

Austromitra angusticostata ———

Austromitra pouciplicata ———--—

Austromitra mulfiplicata—

Ericusa cf ancillcides - ————

Yrosfoer colfeecescfeesees

wena bey

Aphera (Sydaphera) wonnonensis

errata charma —

Serrata weymouthensis

Closia doma

Closia arena) --——— = -

Closia sogma

Sibberula chime

Gibberula tolla

Marginella serateided meta

Marainela Eratoidea)crista

Epidirona adelaidensis

Syntomodrillia ludbrookae

Syntomodrillia sp

omopleura ludbrookac

Reese kee .

urglcus (Euguraleus) adelaidensis —

aiuso [Semiretusa) cansligradota

2tusa (Semirgtusa) cox) —

cynic nd angustata So

ylichna anficingulata

Bamonielia bullagformis —

“Trans. Roy. Sac. S.A.", Val. 87.

@® Denotes type localiiy and depth.

Fig, 4, Vertical Distribution of Mollusca.

Compiled by N.HLudbrook and T M.Stee!

1962.

VERTICAL DISTRIBUTION OF MOLLUSCA

40 350 360 370 380 390 400 410

{eX |

] m

63-196

Hab

Date 6-36:

CORRELATIONS, TERTIARY ROCKS OF AUSTRALIA 13

entitely derived, The molluscan fauna from this section has uot yet heen

studied but # preliminary inspection shows the presence of Miocene elements

such as Kalrigzania,

Late in 1961 during the laying of a pipe line at 5 to 10 feet depth below

the bed of Khe River Murray at Loxtou Mr. M. J, Paul made a valuable collection

of megafossils fom the Boukpurnong Beds at this level, The mollusea inchide

Pinctuda crassleardia (Tate), Miltha hore (Cotton), Cucullaea corivensis MeOoy,

Mytilus cf. linguatulus Tate, Glyeymeris convexa (Tate), Clyeymeris el. catno

zoted (T. Woods), Euerassatella kingicoloides (Pritchard), Neotrigonia trua

Cotton, Cypraeca amygdalina Tate, Wylospira ceoronata (Vate), Palinices

(Polthives) subjugum (Cotton), and Cotlonta et, heplagonatis (Late). ‘This is

a prisdarhiizantly Pliocene assemblage containing the Kalimnan Tylospira

eoronala. The assnetated microfauna is also predominantly Pliovenc. The Bouk-

purnong Beds are therefore here placed higher in the sequence than before and

ave revarded as Upper Miocene to Lower Pliocene in age,

PLIOCENE.

If the Bookpurnong Beds are partially at least of Pliocene age then the

overlying Loxton Sands are entirely Pliocene and not Upper Miocene or Chelten-

hatdan as hitherto tentatively stated (Lucbrook, 1957, p, 179; 1961, p, 89).

As the Loxton Sands are estuarine and contain only shallow water faunas

dominated by Oxtrea. sturtiana they are diffcull toe correlate hivstratigraphically.

No other rocks in South Australia are known to contain the molluscan fauna

ef Uke Toxton Sands (Ludbrook, 1961, p. 73),

The overlying Norwest Bend Formation has been correlated with liime-

slime containing characteristic mollusea such as Anorontia sphericula andl

Cwmpanile triseriale which oceur at many localities Trom Fishery Bay on Eyre

Peninsula to Moorlands in the Murray Basin (Ludbravk, 1959), The Hallett

Cove Sandstone and the Dry Creek Sands of the Adelaide Plains Basin have

been plaved at this level. Authors have in the past used the dime-rock ierm

“Adelaidcan Stage” for the Dry Creek Sands and their fauna. The name was

abandoned because of its confusion with the Precambrian Adclaide System and

ne substitute stage name is now in use, Beeause of its distinctive molluscan

assemblage. T propuse to use the name Yatalan for the fauna of the Dry Creek

Sands and their equivalents, the faunal unit being represented in Dry Creek

Bore from 320 to 410 feet depth, Abattoirs Bure 341 to 500 feet, Croydon Bure

395 te 525 feet, Kanyonga Bores 37] to 562 feet. The eeographical name is taken

from the Hundred of Yatala in whieh many of the bores are located,

The so-called Pliocene of the Adelaide Plains Basin is divisible inta three

members —a basil unuamed silt member which is present in Croydon, Kooyanga

anc other bores (Steel, 1962), the richly fossiliterous pale grey shelly sands

{Dey Creek Sands) from which the foraminifera (Howechin and Parr, 1938)

and the mallusea (Ludbrook, 1954-1958) have been deserilied (the Yatalan

Lets) and ancupper member of fine te medium: quartz sand with a distinctive

assemblage Gf small mollusea, the most common of which are Bittium ( Eubit-

Fire) lawleyanem and a species of Diephoraemactra. The acvomnpanying chart

(Fig, 4) shows the vertical distribution in relation to sea-level of mollusea in

15 bures in the Adelaide Busin to the west of Adelaide, including Cowandilla

hore. From this analysis it is obvious that the Dry Creek Sands with the

Yataliun fauna of large warmn-water mollusca occur below 340 feet below sea-

level and are overlam by s younger member with a distinct fauna from 190

lel N, H, LUDBROOK

feet to 305 fect, Most of the mollusca deseribed by Cotton (1947, 1949) as

will be seen from the chart, came from this member, which is of limited geo-

graphical extent to the west of Adelaide in the general Locklevs area.

The molluscan fauna of the upper member fuhabited a lagoonal enmviron-

ment or very shallow water, Its general composition is similar to that of the

marginal salt lagoons al Lake McDonnell. If the extioction of the warm-water

Yatalan fauna represents the onset of colder conditions at the end of the Pligcene.

then the Pliocene-Pleistocene boundary for the Adelaide Basin should be placed

between the Dry Creck Sands and the upper member occurring in the Lockleys

area. This would be in conformity with the present placiug of the boundary in

New Zealand between the Waitotaran and (he Nukumaruan. The Dry Creek

Sands have previously heen related to the New Zealand Waitdtaran Stage (Lud-

brook, 195+. p. 54).

Sediments overlying the Norwest Bend lormation in the Murray Basin

have oot yet been defined,

REVERENCES

Bava. B. E,. 1963, Palynologicul Repart No. 98, Lake Eyre No, 20 Bore, South Anstridia.

Dept, Mines Geral. Survey Report Invest. No. 24 Appendix (im press).

Cauwrrn, A. N.. 1958. Peludie Foraminifera in the “Lertiary of Victoria. Geol, May.. 93 (4),

pp. 297-304.

Canna, ASN, 195), Guide Foraminifera of the Tertiary Stages of Vietaria. Vie, Min.

Geol. Joun., 6 (3), 1958/1959, pp. 48-51.

Corron, B.C, Li47. Some Tertiury Fossil Mollnses from the Adchiidern Stace (Pliocene }

of South Australia, Ree, 8. Aust, Mus, 8 (4), pp, (53-670.

Gorrox, B. G., 1949. Australian Recent and Tertiary Molhises Family Murginellidae. Ree.

5, Aust, Mus,, 9 (2), pp, (97-224, pls, 17-20.

Crrapim, 1, 1956, Fossiliferous Hocks from the Nullarbor Plains. Papers on Tertiary Micro-

palaeontulogy.. Dept. Nat. Devel, Bir, Min, Res. Geol, Geoph, Rep, No. 25, pp. 26-42.

Eames, F. E,, Bawsxor, FLT. Brow, W. UL, and Crance, W. J, 1962. Pundamentals of

Mid-Tertiiry Stratigreplical Correlation, Caorbridge University Press, pp. 1-15], pls,

I-XVIT, lus, 1-20,

Orausswen, M, FP. and Paros, L. W. led.), 1958. The Geology of South Australia. Jorrn.

Creal, Sne. Aust. 5 (2), pp. 1-163, figs. 1-26, pls, 1-11. maps A-D.

Hounmuoox, N. ae R,. $953, ‘Tertiary and Recent Marine Ostracoda of New “Zealaucd. NZ.

Geol. Surv. Pal. Bull. £8, pp. 1-83, pls. 1-18.

Howcris, W.. wil Pans, W. J, 1938. Notes on the Geological Features and Formniniteria

Fauna of the Metropolitan Abattoirs Bore, Adelaide. Trans. Roy. Soo, S. Aust., 62 (2),

pp. 287-317, pls. 15-19.

Jenkins, D. G., 1960. Planktonie Voramninifera tram the Lakes Entranee Oil Shaft, Victurie,

Australia. Mitropaleontulogy, 6 (4), pp. 345-3971, pls. 1-5, tent figs. 1-10.

Lupimeoor, N, H.. 1954-1958. The Mollisean Faima of the Pliceene Strata Underlying the

Adelaide Plains, Part 1, Trans. Roy. Sac, 5, Aust., 77, pp. 42-64; Part 11, 1955, id. 87,

pp. 18-87; Part UI, 1956, ic, 79, pp. 1-36; Part IV, 1957, id., 80, pp. 17-58; Purt V,

1958, il, pp. 43-111.

Luppeook, N, H., [fdde. Reconmissance Survey of the Eucla Basin, Stratigraphy and

Palaeemtology. Dept. Mines 8. Aust. Geol, Sary. Pal, Rep (unpublished).

Lopprook, N. H., 195db, Au Snterpretation of the Tertiary Sequence Between Wilson

und Maralinga in the North-Eastern Portion of the Eucla Basin. Dept. Mines 5. Aust.

Geol. Surv. Pal. Rep. 3/54 (ainpublished ),

LupsHoos, N, H., 1956. Palwontelogical Dxunination of Material. Hydrological Investiga-

tious, Yaluta Station. Samples FO04/56-F119/56 (uripublished ).

Lunmoor, N. ID, (957. A Referenee Column for the Tertiary Sediments of the Smuth Aus-

tralian Partion of the Murray Basin. Jeurn., Proc, Roy, Soe, N'S.W., XC. pp. 174-180.

CORRELATIONS, TERTIARY ROCKS OF AUSTRALIA 15

Lupunoox, N. H., 1958. Stratigraphic Sequence in the Western Portion of the Fucla Basin.

Joum. Roy. Soc. West Aust, 41 (4), pp. 108-114.

Lupsroox, N. H., 1959a, A Widespread Pliocene Mollnscan Fauna with Anodontia in South

Australia. Trans. Roy. Soc. 5. Aust., 82, pp. 219-233, pls, 1-3,

Lununoox, N. H., 1959b, Material from the Western Portion of the Eucla Basin, Dept.

Mines 8. Aust. Geol. Sury. Pal. Rep. 5/59. G.S8. 1343 (unpublished),

Lupnroox, N. H., 1959c. Exvil Pty, Ltd, Palaeontological Examination of Material from and

North of the Eucla Basin. Dept. Mines 8, Aust. Geol, Sury. Pal, Rep, 9/59, G.S, 1514

(unpublished).

Luyonoox, N. H., 1960. Exoil Pty. Ltd. Eyre No, 1 and Gambanga No. 1 Wells, Sub-

surface Stratigraphy and Micropalacontological Study, S. Aust. Geol, Sury. Pal, Rep.

11/60. G.8, 1876 (unpublished). In press, 1963, Bur, Min. Res, P.S.S.A. Series.

Lunproox, N. H., 1961. Stratigraphy of the Murray Basin in South Australia. Geol. Surv,

S, Aust., Bull. 36, pp. 1-96, tables I-XI, pls. i-viii, text figs. 1-36.

Tamsnoox, N. U., 1963. Exploratory Drilling, Lake Eyre. Subsurface Stratigraphy. Dept.

Mines S.A. Geol. Surv. Rep. Invest., No. 24. Appendix (in press).

Revnoups, M. A., 1953. ‘Vhe Cainozoic Succession of Maslin and Aldinga Bays, South Aus-

tralia, Trans. Roy. Soc. S. Aust., 76, pp. 114-140.

Sincteron, F. A., 1941. The Tertiary Geology of Australia. Proc. Roy. Soe. Viet., 53 (1),

ns., pp. 1-125, pls, 1-3.

Sreec, T. M., 1962, Subsurface Stratigraphy in the Western Suburbs of Adelaide. Geol.

Surv. §. Anst. Quarterly Geological Notes, No, 3. April.

Svinron, R. A. Tenrorp, R. H., and Mitter, A. H., 1961. Cenozoic Stratigraphy and

Vertebrate Palaeontology of the Tirari Desert, South Australia. Rev. S. Aust. Mus., 14

(1), pp. 19-61.

THE BRUSH-TAILED OPOSSUM OF KANGAROO ISLAND,

SOUTH AUSTRALIA

BY H. H. FINLAYSON

Summary

Trichosurus vulpecula from Kangaroo Island is compared in series with the animal from the

adjacent mainland of the Adelaide district and is found to be subspecifically distinct, and named

T. v. raui. The evidence is presented in detail.

THE BRUSH-TAILED OPOSSUM OF KANGAROO ISLAND,

SOUTH AUSTRALIA

By H. H. Fintayson

[Read 9 August 1962]

SUMMARY

Trichosurus tulpecula trom Kangaroo Island is cormpared in serics with the

animal from the udjacent mainland of the Adelaide district and is found to be

pulsepecitiaally distinct, and named T. 4, ravi. The evidence is presented in

detail,

INTRODUCTION

In his Ireatment of Trichosurus vulpecula Kerv in the “Mammals of South

Australia”, Wood Jones (1924, pp, 196-203) gave a succinct account of what he

considered were the essential differences which separated the animal of Kan-

garoo Island fram that of the adjacent mainland, Je was especially familiar

with the island form through his intimate connection with Flinders Chase and

his frequent visits to that sanctuary at the western end of the island, where

for a time the dense opossum population was kept within bounds by an annual

snaring for the fur market.

It is clear from his account that he regarded the Kangarog Island opossum

as a distinct geographical subspecies, as he compared und constrasted it with

what be called “the typical variety as it occurs round Adelaide”. He did not,

however, give a formal definition nor apply a distinguishing trinomial to it,

and ihere now scems reason to believe that the prepared specimen on which

he chiefly relied for his description was soméwhat atypical of the population

(infra).

In August, 1925, the prescut writer made a visit ta the Chase in company

with the Taxidermist of the South Australian Muscum, and with the assistance

of the then Ranger, Mr. Harold Hansen, collected a satisfactary series of opos-

sums, which were measured and weighed in the flesh and preserved in the

conventional ways. This collection was deposited in the South Australian

Museum and, together with specitnens in my own possession, forms the basis

of the present account.

The qnestion of what are the true characters of the “typical”, primary, or

nominale race of T. nulpectula is easier to ask than to answer, and many similar

questions continue to bedevil the trinominal treatment of early deseribed species

which like it have no surviving hololypes nor modern descriptions. That it

came from the immediate or near vicinity of Sydney in New South Wales is

probable but the currently accepted view. which stems from Iredale and

Troughton (1934, pp. 30-31), that T, culpeeula vulpecula occurs over the greater

part of south-eastern Australia, including southern Queensland, New South

Wales, Victoria und South Australia, is more in the nature of a working hypo-

thesis than an established fact.

Trans. Roy. Soc. §, Aust. (1963), Vol, 87,

18 lt. H. FINLAYSON

However, this wneertainty does not invalidate the real differences which

separate the two populations studied by Wood Jones which have been wmply

confirmed and extended in the present work, and which appears to place the

Kangaroo Island form morphologically further from that of New South Wales

as tar as it is known, than from that of the Adelaide district. Unlike most other

present day insular oeeurrences of the species in South Australian waters, which

are either known to be due to deliberate introduction or are ander suspicion

of such, the Kangaroo Island population is undoubtedly indigenous, of large

exteut both numerically and territorially and of homogencous character. It has

heen isolated from that of the adjacent mainland for a perigd generally esti-

mated at 10,000 years at least, and possibly much Ionger. To continue ta deny

it trinomial distinction is more likely to confuse the general overall conveption

of the radiation of the species, than to clarify it, and for these reasons I propuse

to define it us follaws:

Trichosurus vulpecula raui® subsp. nov,

An insular subspecies from Kangaroo Island, St. Vineent Gulf, South

Australia.

General characters similar to those of the population of the Adclaide district

and south Mt. Lofty Range of the adjacent mainland (currently regarded by

authors as representing T. celpeeitn vulpecula Kerr), but distinguished hy:

its larger size, richer pelage, and somewhat darker and colder darsal colouration,

Yhe dark markings Gf the head and hind foot are larger. more saturate and

conspicuous, and the black portion of the tail brush is longer.

The skull is longer, relatively narrower wid with narrower nasal bones, and

shows other differences noted below.

In the dentition, the molar rows are lonver, Ms'~* in adults yielding an

approximate mean of 13-1 mm, as against 13-9 mim, on the mainland,

Type Locality: The serubs of Rocky River in the sanctuary of Flinders

Chase at the western end of the island.

Typ: Filled skin arid skull of a young adults, South Australian Museum,

segistered number M.2518. Collected August, 1928. A series of contemporary

topotypes is also registered. Thirty specimens examined,

Dimensions of Type (for definition of dimensions see below): Head and

body, 435 mm. tuil, $20: pes (total s.u. length), 71; pes (length of naked sole

sae), Gl; ear, lenvth, 356; ear, breadth, 28; weight in grammes, 2,270.

Skull Dimensions of the Type: Basal length, 77-7; zygomatic breadth, 51-4:

nasals, length, 34-0; nasals, greatest breadth, 14-0; interorbital constriction, 10-1;

palate Jength, 46-0; anterior palatal foramina, 6-0; basi enanial axis, 24-4; busi

facial axis, 53-5; facial index, 219: Ms.) #, 15:8; P*, 4-0.

EXAMINATION OF THE MATERIAL

South Anstralian mainland material, available for comparison with the

island form, is copious, but much of it is only broadly localized and probably

comes from Jocalities considerably north of Adelaide und in drier clistricts

where. as Wood Jones bas shown, the size falls off considerably, Preliminary

tests. having shown it to be much ino heterogenecons for treatment en bloc, a

7 Commemorating the late FJ, Ran, for many years Taxidermist of the: South Australian

Museum, amd a senior member of a family which bas rendered conspicuous service tu that

eralt in’ Anstratia.

BRUSH-TAILED OPOSSUM OF KANGAROO ISLAND), S.A. ty

restricted sample from the Adelaide-Wakefield Plain (including the urban area)

and the south Mt. Lofty Range, was selected comprising abont 25 specimens in

guod condition and sufliciently documented for the purpose.

The age criterion adopted was the closure of the hasioccipital-basisphenoid

suture, which, though it takes place fairly early, yet serves to exclude obviously

immature examples, and gives a sample of fairly uniform size. This test re-

duced the Kangaroo Island series to 14 examples (74 ;79), and the Adelaide

district one to 13. (5.2 : 32 :4 not sexed),

Fugsi Dryrenstons

The range and approximate mean of seven items under this head are quoted

for the Kangaroo Island series in Table 1.

(a) The head and body length represents the total Jength of the dorsal

contour measured with a steel tape from the wpper extremity of the rhinarium

to the end of the tail excluding the terminal hair tuft, minus the length of tail.

(b) Tail length is fram the cloaca to apex (cxeluding hair) measured along

the ventral surface with the tail stretched at right angles to the trunk,

heel to the extremity of the most distant apical pad and therefore ‘excluding the

cluw.

(d) Length of sole of pes represents the nude portion of the above,

(e)} Ear length is the distance from the bottom of the tragal notch to the

apex of the pinna, taken with the zero of a rigid rule, with the notch,

(£) Eur breadth is the greatest transverse breadth across the trough of the

pinuu, at right angles to the above,

(g) Weights were ascertained on removing animals fram neck snares ap-

proximately 6-10 hours post mortem,

TABLE |

{ Cambinect

7 Adult + 6 Adult 4 Adult ¢+=

Head and body | 410-400 (442) 415-485 (450) ATU-4A8S (146)

Tail 20-850 (319) 290-340 (Hh1) | 2-380 (315)

Pos (turtive 10.) 62-74 (BS) fi) -fi44 (85) | BTS (67

Pes (nade sole only) S5-H1 (a7) | 95-a7 (5b) | 55-G1 (57)

Ear lenoth 13-59) (AG) 42-58 (ph) | 59-59 (54)

Bar breadth | 27-8) (28) 28-31 (2) j 27-31 (28)

Weight (in grammes) 1,816-2,724 (2335) | 2,043-2,724 (2.406) 1816-2724 (2,370)

Range and approx. mean of flesh dimensions in Uvichasurna onfpecule rand sulisp. nev,

The question of the relation ot the external dimensions of the populations

from the island and the Adelaide district has had to he left in abeyance owing

to lack of data for the latter, sufficiently adequate to justify a comparison. Most

of the published figures for the species are doubtfully’ comparable with the

above, having heen derived (rom stuffed skins or by methods based on uncertain

landmarks. The lengths of pes quoted in literature are particularly dubious,

suggesting in some cases that the measurement made was actually of the nude

portion of the plantar surface only, which (as shown above) may be a full LO mm.

less than the true dimension from the caleaneum.

a) H, H, FINLAYSON

Wood Jones (op. cit.) considered the island form to be larger than that

of the Adelaide district and the evidence of cranial dimensions reviewed below

supports this, but it should be noticed that the male measured by him is (in

respect to head and body length at least) excessively large, exceeding the

maxima of the series here measured by 15 p.c.

PELAGE

In general characters the pelage of the Kangaroo Island opossum is (nite

similar to that of the Adelaide district, exhibits a similar range of variation and

u proportion of each series is scarcely distinguishable in this regard. There are,

however, valid average distinctions, and where these are most decidedly de-

veloped the total dissimilarity may be considerable. Variation dure to seasonal

and age changes are marked in both groups, but if these arc climinated by

i ining the comparison to adults in mid-winter coat, the tollowing distinctions

WOH:

(1) The dorsal pelage in the Kangaroo Island anitaal is darker in tone and

colder in hue, the neutral grey being modified towards glaucous rather than

fulvous. The length of the ivory or white subterminal band of the fur is also

less and the grizzling of the dorsal coat correspondingly finer. Aged males are

sometimes strongly reddened on the fore back as in the mainland animal, but the

latter distinction remains.

The male described by Wood Jones (which is now in the South Australian

Museum collection) is an extreme example of this secondary reddening, but a

warm tawny dorsal colouration is not characteristic of the series as a whule:

quite the contrary in fact.

(2) Ventrally the two series show comparatively slight differences, bath

being generally distinctly buffy in external colour. “In the island graup the

culour possibly averages a little warmer, being near Ridgway’s ochraceous butf

in the richest examples, but the “rusty” belly mentioned! by Wood Jones is only

shown by one or two aged males in the present series, and is partly due te an

unusual extension posteriorly of the brown colouration of the sternal gland site,

which may oecur in mainland examples also,

(3) There are considerable differences between the two series, in the

extent and intensity of the dark markings of the head and feet. Im the Kan-

gatoo [sland form the dark pateh at the base of the car backs is increased in

area, so that the upper white or bull portion is sometimes reduced to a narrow

ship on the posterior upper murgin— the colour is generally darker and mire

snturate also; a dark brown black approaching jet black in some examples.

Similarly, in the pes the dark jrregulay markings on the tarsus and the dirk

fringe around the heel and on the outer margin of the foot are increased in

ure and density and invade the dorsum over the metatarsals, giving a more or

less strongly pied effect ta it, in which the light coloured «rey or buff areca may

he Jessy than half the whole.

In the Adelaide series the markings of the foot are not strongly developed

andl usually the entire dorsum is pale.

(4) The brush of the tail is better developed in the island animal and the

Iilavk portion more extensive in relation to the grey, always covering more than

half and sometimes three-quarters ot its total length. Iu the mainland analogue

it is frequently Jess than half the total length,

BRUSH-TAILED OPOSSUM OF KANGAROO ISLAND, S.A.

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22 If, I. FINLAYSON

Crantar CHanactens

Seventeen dimensions and indices were examined in the two groups and the

mor conventional are summarized in Table 2. In absolnte dimensions the

nitiges overlap in most items, but the approximate means tor the Kangaroo Island

sevies are almost always higher, and in the chief longitudinal dimensions by

9-6 pre

The Kangaroo Island skull is generally narrower zygomutically, the breadth/

wreatest length ratio giving a mean of 59°35 as against 61-8 in the mainland

skull and the nasal bones are also narrower with a breadth index of 44-7 as

against 48:7. The interorbital breadth and length of anterior palatal foramina

are iso relatively slightly less.

A visual impression that the skull of the island animal was longer muazled

could not be substantiated by an appeal to the cranial index, except in the male

group. The basisphenoid-prespheuoid suture in almost all skulls examined was

abseured by overlapping plates of the pterygoids, und as a substitute landmark

in the determination of the index, the apex of the visible portion of the husi-

sphenoid was used. Although this frequently coincides with the position of the

suture, it proved a somewhat erratic feature, and the figures for the index and

the originating, axes are approximations. only, Au approximate rostral index

derived from the length of nasals in relation to greatest length of skull confirmed

a slightly increased length of muzzle in the Kangaroo Island males only — these

are also slightly narrower in the muzzle.

In non-metrical characters, variation in both scries is high, comparatively

small age changes effecting considerable differences in general appearance,

especially in the frontal and interorbital region; however, the differences de-

tected mictrically are often quite apparent visually, The foramen magnum in

Tc. raui is decidedly larger both abschately and relatively and is deeper from

above downwards than in the Adelaide series.

Drntition

The upper molars and upper secatots only were examined quantitatively,

and the former provide one of the most useful and constant distinctiims hetween

the two series, In the Kangaroo Island race, the length of Ms! * in situ yields

u range of values almost entirely above that for the mainland serics and an

approximate mean which is 6 p.c, higher.

O. Thomas (1888, p. 187) used the length of the molar rows in his key of

chaiaeters differentiating “T, tulpecela fypiens” on the one hand from T. bv.

fuliginasus and T. caninus on the other, the former having a length of Ms! 4

in situ of less than 14-5 nim, and the two latter more than 14-3 mm.” The main-

land population from the Adeluide district here studied conforms approximately

to Thomas's definition, giving a range for Ms!~* ot L3-1-14-6 (13-9) mm. in

adult skulls: but the Kangarov Island group (though nmvuch closer to that of

the mainland in all other vharacters than to that of Tasmania) approximates the

latter in its longer rows with a range of 14°4-15-7 (15-1),

REFERENCES

Dimmer, G. ML. 1986, CSI. Wildlife Researeh, 1, pp. PAL,

thebank, To. and Trovuaiiros, Kook G., Loe, “Checklist of Manuals Recordect trem Ars

THE LARVAE OF AUSTRALIAN DYTISCIDAE (COLEOPTERA)

BY C. H. S. WATTS

Summary

The larvae of eighteen species of Dytiscidae are described for the first time. These are Bidessus

bistrigatus, Clk., Bamabilis Clk., Hyphydrus australis, Clk., Sternopriscus cluvatus, Wehn.,

Paroster insculptilis, Clk., Chostonectes latus, Sharp, C. nebulosus McLeay, Antiporus gilbertii,

Clk., A. femoralis, Boh., A. blakei, Clk., Necterosoma penicillatus, Clk., N. dispar, Germ., N.

wollastoni, Clk., Macroporus gardenerii, Clk., Platynectes decumpunctatus, Fab., Lancetes

lanceolatus, Clk., Copelatus extensus, Sharp, and Homoeodytes scutellaris, Germ. These include

the first descriptions of larvae of species belonging to the following genera: Sternopriscus Sharp,

Paroster Sharp, Chostonectes Sharp, Antiporus Sharp, Necterosoma McLeay, Macroporus Sharp,

Platynectes Reg. and Homoeodytes Reg. A key to the genera of Australian Dytiscids using larval

characters is given. Notes on the rearing of Dytiscid larvae and the method of feeding in Copelatus

are included.

THE LARVAE OF AUSTRALIAN DYTISCIDAE (COLEOPTERA)

by C, EH. S, Warrs®

(Communicated by Dr. 8. J. Edmonds)

[Read 9 Angust 1962]

SUMMARY

The Jarwie of cighteén species of Dvtiscidae are desurihed for the first

time. These are Bidessus bistrivatus, Clk. Bumabilis Clk, Uyphydius australis

Clk., Sternopriscus clavatus, Wehn,, Paraster aseulptilis, Clk, Chostonectey lutus,

Sharp, C. nebulosus MuLeay, Antiporus gilbertii, Clk, A. femoralis, Bah, A,

blakei, Clk.. Neeterosoma penicillatus, Clk. N. dispar, Germ., N. wollastoni,

Clk, Maeroporus: gardenerii, Clk., Plutynectes decumprmetatus, Fal,, Lancetes

lanticolatt, Cik., Copelatus extensus, Sharp, and Homoeudytius sxeutellaris,

acru.

These include the first descriptions of larvae of species belonging to the

follawing genera: Stertopriscys Sharp, Paroster Sharp, Chostonectas Sharp,

Anéiporus Sharp, Necterosoma McLeay,. Macronarus Sharp, Pletanectes Reg, and

Homneodytes Reg A key to the genera of Aostratinn Dytiseids using larval

characters is: given. ‘

Notes on the rearing of Dytiscid Inrvae and the method of feeding in

Copelutus are eluded,

INTRODUCTION

The Dytiscidae of Australia have received little attention since Sharp's

mondgraph in 1552, and 1 do not know of any published description of the larvae

of an Australian species. However, the larvae of some Northern Hemisphere

species, belonging to genera that are represented in Australia, have been de-

scribed. Some of them differ in important characters from Australian species in

the sume genus.

The Australian region is especially rich in Hydroporinae, most of our genera

in this group being endemic and the discovery of the larvae of these genera fills

a large gap in our knowledge of the larval [lydroporinae. This is not so trne

of the other groups; there are few endemic genera, and most genera inclnde

non-Australian species, whose larvae have already been described. In these

groups, larvae from all but two genera have been described from outside Aus-

tralia, The two genera for which larvae have been described for the first time

in this paper are Homocodytes in the Cybistrinae and Platynectes in the Colym-

betinac, The first is endemic to Australasia; the second is wide-spread throughout

Australasia and South-East Asia,

The following descriptions are based on exuvia of last instars of larvae

that have beeu reared through to the adult stage in small aquaria made from

two pelvi dishes, The aquariury itself was simply the bottom of a small petri

dish which was placed inside a mueh larger petri dish bottom, and the

space around it filled in with damp sand. With the inner dish full of

water and the lid of the larger dish in place, the sand remained moist. Under

Trans. Roy. Suc. §, Aust. (1963), Vol. 87.

24 C. 1. S. WATTS

and eventually pupated in the surrounding sand. Apart trom feeding the larvae

and removing carcases, these aquaria need little attention and tuke up very

little space, The Jarger lurvae are mostly cannibalistic and have to be kept

separate, but the smaller Hydroporinae and some larger larvae such as Copelares

ean be kept together quite safely, With the Hydroporinae | found it neces-

sury to put some cotton wool in the aqnaria, as this makes it easier for them to

capture their prey. Toused cotton wool in preference to alyae or other plant

material as the Jatter die quickly in such small containers and soon foul the

water. Dead prey, if at all Unie, will also foul the water quickly if not removed.

All the following species have been reared in aquaria of this design with

few failures. In captivity the larvae were fed on mosquito, chironomid and

dragon fly larvae or Daplinja, The actual prey used depended on the size of

the larvac. The only genus that has proved difficult to breed under these

conditions has been Copelalus, where, out of a total of five species and numeruns

specimens, only one adult has becn reared. In most cases the mature larvae

have ctawled out on to the sand but have wot papated or even attempted to

construct a cell, It seems, therefore, that the conditions necessary for pupution

tii take place in this genus were lacking.

STRUCTURES USED 1N THE CLASSIFICATION

In the Hydroporinae the most useful tixmmwmic characters are ta be found

in the form of the frontal projection and the last abdominal seament, the shape

of the Jabiim and the atrangement of setae on the cerci.

The frontal projection is a projection from the front of the head and is

nsed to help hold the prey during feedinu, the prey being held against it by

the mandibles which are strongly curved upwards in this group, The frontal

projection is relatively simple in genera such as Hyphydrus (Fig. 10), although

even in this genus it is furnished with lateral teeth. In others it is a more

complex structure, In Paroster (Vig, 8) and Sternopriscus (Fig, 9) there ts a

weak projection from the side of the main structure, this projection heing better

developed in Chastonectes (Fig. 8) and in Antiporus (Wig, 1). 1 lwe called

it the lateral projection. When the lateral projection is small as in Parester it gives

the frontal projeetion the appearance of being notched, In the more developed

forms such as Anfiporus this effect ts fost, but L have still ased the term

“notch” in referring to the space between the frontal projection and the lateral

plojection, I most species there are well-developed teeth on the underside

uf the frontal projection, the majority being near the tip but they often extend

hbuckwards along the margin, as in Bidessux (Fig. 7) or on the margins of the

lateral projections, e.g, Chostonectes.

In some genera the larvae have a pair uf spines on the underside of the

treonlal projection as well. These are very small in Chostanectes, Necterosema

antl Macroporous, but are large in Anfiporus, especially A. gilbertii: (Fig. 1)

where they are placed on the top af a downward oulgrowth from the frontal

priyection (Fig, 18).

The last abdominal segment is often produced into a long tube with the

spiracles ut its tip. 1 have used the term siphon in referring to this elongation

which is usually well marked of From the rest of the segment, In genera

suule as Myphydrus where Ht is not clearly marked off from the rest of the

segment, | have taken it to end appesite the base of the cera, The length of

the siphon varies a lot, being long in Macroporus and Chostonectes (Figs. 25.

27), but virtually absent in Sternepriseus and Antiporus (Pigs. 15, 25),

Tn most Dytiscid larvae there are a yew of stout spines along the Literal

qiaevin of the head: these are the temporal spines, In the genus Agabus, fron

LARVAE OF AUSTRALIAN DYSTICIDAE (COLEOPTERA) 25

the Northern Hemisphere, they lie on a line that, if extrapolated forward, would

pass well below the ocelli; in all the known Australian genera with the exception

of some Hydroporinae they lie on a ling that will pass through or just below the

ocelli. Temporal spines are absent from the Bidesseni and Paroster and ure

poorly developed in the other Hydroporinac.

The shape and orientation of the maxillary stipes are characters useful in

the classification of most groups, as are the shapes of the labium and its ligula,

if the latter is present. The maxillary stipe may be either long and thin or short

and thick, In the first case the galea, which in this family is reduced to a

finger-like process, is rather small and inconspicuous; in the second case it is

larger and is usually a very noticcable part of the maxillae. In some genera,

e.g, Lancetes, the stipes have a number of small hooks on their inner edge; in

Copelatus these are large and slender and are placed directly below the galea.

The labium is wider than long in most Dytiscid larvae, other than the Hydro-

5 6

AP Nf NY

Poatre 1

Figures 1-9. Line represents -1 mm, Fromlal projections of (1) Antiporus gilbertii,

Clk. ventral surface; (2) A. blekei, Clk., ventral surface; (3) A. femoralis, Boh., ventral sur-

face; (4) Macroporus gardnerii, Clk., dorsal surfacc; (5) Chostonectes nebulayus, McLeay,

dorsal surface; (6) C. latus Sharp, dorsal surface; (7) Bidessus amabilis, Clk, dorsal surface;

(8) Paroster insculptilis, Clk., dorsal surface; (9) Sternopriscus clavatus, Wehn, dorsal surface.

26 ©. H. & WATTS

porinae, where it is usually slightly longer than wide, or sometimes much longer,

as mm the Hyphidrini, A ligwa, which is a projection forward from the front

of the labium, is present in several genera. Lt varies greatly in develupment:

ut ove extreme it is small and naked, e.g. Momoeodytes; at the other long and

spiny, eg. Rhantaticus.

The cerci wre af yery yatiable length. They are usually long but the length

vitties a lot hetween species and between geneva. They may have only a few

long setae which are usually placed in whorls, or they may have a Jot of smaller

setae irregularly placed along them. The former condition is often referred to

as “veret with primary hairs”; the latter “cerci with secondary hairs”. In some

species, mostly among the Hydroporinae, the cerci are made up of two parts.

The basal part is robust and bears. setue; the apical part is devoid of setae and

is often very fragile, There ure great differences in the relative length of these

differeut parts, In some, the apical portion is reduced to a small knob, e.g.

Platynectes; in others it is long and thin und gives the impression of being a

very thick apical seta, In species with a slender apical portion, i. Bidesyus

spp., the faction between the basal anel apical portions is weak and the apical

portion is often broken off.

The key to the genera has been drawn up from the characters visible in

unmounted material, Jn order to give as complete a key as possible, several

genera, indicated with an asterisk in the key, are included which [ have not

seon, The characters used in these cases arc from published figures and deserip-

tions of Northern Hemisphere species and might not apply to Australian species.

The key thus produced includes twenty out of the twenty-five Australian genera.

Where measurements are given these refer to the last instar larvae, unless

otherwise stated, It should he remembered that these larvae show «a lurge

increase in length during an instar, and also, that whereas spint specimens aire

often in a rather contracted condition, mounted specimens are often expanded,

The Jeneth rrieagurements are therefore meant as a rough guide only. They

were mide from spirit specimens. thal appeared to he full grown dash hostar

larvac ina more or less natural condition. he lengths viven do not inehide the

cerci, The lengths of head capsules of the Hydroporinae include the Hontal

projection.

KRY TO TILE GENERA OF AUSTRALIAN DYTISCIDAE BASED

ON TIVE CHARACTERS OF LARVAE*

Head with frontal ptojection (Fig. 18): maxillary palps 3-segmented

( Ilvdroporinae)

1. Head without frontal projection; maxillary palps more than 3-segmented — 1

2, Frontal projection without lateral projections

2.. Frontal projection with lateral projections

%. Labium short and broad, Siphon Jess than twice the length of the rest

of the segment £ a ; " a i. 5 I 0 ‘t

8. Labium long (Fig. 19). Siphon more than twice the Jength of the rest

of the segment (Iig, 24). 7 Hyphaydees

4d. Larva not greatly widened, Vrontal projection short and wide,

with numerous Jateral teeth extending nearly to base (Fig. 7)

Bidesstrs

4, Larva greatly widened in middle. Frontal projection clongated,

with only a few lateral teeth restricted te apical half Aydrovatys®

Last abdominal segment nol greatly elongated, siphon less than twice

the Jength cf vest of sezment " if 4 eo 7 6

wmusis

"The asterisk indicates that I have not seen a larva of any species from these wenera.

13.

15.

17.

LARVAE OF AUSTRALIAN DYSTICIDAE (COLEOPTERA )

Last abdorninal segment greatly elongated, siphon more than twice the

length of rest of segment (Fig. 25) ws Macroporus

6. Width of notches on trantal projection equal to, or greater than,

width of frontal projection between the notch bases

6. Width of notches on frental projection less than width of the frontal

projection between notch bases -

Apical segment not, or only slightly, produced into a siphon (Fig. 98),

Paired spines on underside of the frontal projection well below notch

bases ~_ _ Antiporus

Apical segment produced into a short siphon (Fig. 97). Paired spines

on underside of the frontal projection on a level with or just below

notch bases... Chostonectes

8. Apical segment produced into a short siphon

8 Apical segment not produced into a short siphon (Fig. 15)

Sternopriscus

legs short and stout; notch in [rontal projection slight (Fig. 9). Labial

palpi 3-segmented (Fig. 21) Paroster

Leys not short and stout; notch in frontal! projection larse (Fig. 11).

Labial palpi 2-segmented (Fig, ah Z __ Necterosoma

10. Maxillary stipe short and broad

10, Mavillary stipe long and narrow ~

Cerci absent. or rudimentary. Antenna §-segmented

Cerci present, antenna 6-segmented H yclutic us®

12, Ligula short (Fig, 32) lobes on front of head strongly dentate

(Fig, 38) d 4 Horocodytes

12, ligula long, lohes-on front-of head not strongly dentate. Cybister*

Ligula absent, last abdominal segment without Jaterd fringes of long

setae

Ligula present, Tateral fringes of long setae on last abdominal segment

I4. Ceérei very short, less than length of Jast abdominal segment

(Fig. 26); mandibles tuothed on inner edge. Capelatus

14. Cerci as long as or longer than last abdominal segment; mandibles

not toothed ;

Cetci more than twice the lenuth of the last abdominal gegment with

numerqus setae

Cerci about the same length as the last ahdurtcinal segment, “with; a few

or with numerous sctac

16, Last abdominal segment produced into a brnall siphon: last joint

of antenna less than balf the length of the third joint .. Laccophilus*

16. Last abdominal segment truncate at the apex (Pig, 22); last joint

of antenna more than half the length of the third joint (Fig. 35)

Lancetes

Last joint of antenna more than two-tlurds the length of the third jeint

(Wig. 36); cerci with numerous setae; underside of head with small

spincs _ " Bhantits

Last joint of antenna less than half the length. of the third joint; cerci

with a few long setae (Fig. 23): underside of head without spines

Platynectes

18. Ligula short with four spines. = Eretes*

18. Ligula long, nearly the length of the first joint of the labial palpi,

wiih six spines if Rhantuticus”

* The asterisk inchcates that I have not seen a larva of + auy species from these geuera.

28 C. if, S. WATTS

HYDROPORINAE

Cenus Binrssus Sharp

Head wide with no well-marked neck region and without temporal spines.

Frontal projection wide, with a ventral row of strong teeth around lateral margin.

Antenna short; labium bilobed. Siphon short, about half the length of the rest

of the segment. Cerci variable, either with 4 few long setae or with numerous

shorter ones,

The presence of cerci with only a few setae (primary hairs) was previously

thought to be a generic character, The presence of cerci with numerous setae

(secondary hairs) in B. bistrigatus, Clk., indicates that this character is only of

specific rank as far as Bidessus is concerned,

Bidessus bistrigatus, Clk.

(Fig. 13)

Dorsal surface pale yellow-brown, temporal sutures bordered with dark

brown. Ratio of length of siphon to length of rest of last segment, 1/2-2, Cerci

eight times length of siphon, covered with numerous setae. Ralio of basal

portion to apical portion of cerci 5:2/1.

Length, 3-6-3:8 mm. Head capsule, -57 mm. wide, -76 mm. long,

Larvae collected from a concrete drainage ditch, Canberra, Jauuary 1961,

and from a sheep trough, Adelaide, March 1960.

Bidessus amabilis, Clk,

(Figs. 14, 7)

Dorsal surface dark brows, arca enclosed by temporal sutures and frontal

projection paler. Ratio of length of siphon to length of rest of last seement

1/1-8, Cerci short: 4+5 times length of siphon, with about six long setae, Ratio

of basal portion to apical portion of cerci 1/1.

Length, 3-6-3-9 mm. Head capsule, +62 mm, wide, +78 mm. long,

Larvae collected from Hobart, August 1961; a salty pool, Robe, South

Australia, August 1961; 4 pool with decaying leaves, Cradle Mt., National Park,

Tasmania, January 1960; und a weedy ditch, St. 1elens, Vasmania, Januarv 1962.

Genus Hypayprvus II,

Head small, body compact, and with a hunch-backed appearance. Frontal

projection long and thin, with fine teeth on ventral margins of wpper two-thirds.

Labium greatly elongated. Siphon clongated, about twice the Jengtl of the rest

of the segment. Cerci short with numerous strong setac.

Hyphydrus australis, Clk.

(Figs. 24, 19, 10)

Compact, with a pronounced lump-backed appearance. Black; frontal

projection, middle of head, a baud across the prothorax, abdominal segments

5, 6 and 7, tip of siphon and cerci, and underside, light brown. Body densely

covered with fine setae. Frontal projection and last abdominal segment as

in Figs.

LARVAE OF AUSTRALIAN DYSTICIDAE (COLEOPTERA) 29

Length, 7-9-§-1 mm. Head capsule, last instar, -80 mm. wide, 1-26 mm,

long, second instar, -55 mm, wide, -85 mm. long.

The larvae were collected from a small pool full of decaying leaves at

Stanthorpe, Queensland, January 1961; in a grassy pool 30 miles S.W. of Can-

berra, January 1961; and in a slow flowing creek full of the algac Nitalla sp,

new Adelaide, December 1960.

[ ;

) vet \ |

i 12

ly lia) l

Mia ;

¢ \

k~ 2

Ky “| \ l

16 \7

PLatre 2

Figures 10-21, Line represents «1 mm. (10) Frontal projection of Hyphydrus australis,

Clk., dorsal surface; (11) frontal projection of Necterosoma dispar, Germ.; (12) labium and

labial palpi of N. penicillatus, Clk.; (13) last abdominal segment and cerei of Bidessus bis-

trigatus, Clk.; (14) last abdominal segment and cerci of B. amabilis, Clk.; (15) last abdominal

seyment of Sternoprisous clavatus, Webn.; (16) epistome of Necterosome penicillatus, Clk.;

iy epistome of N, dispar, Germ.; (18) lateral view of head of Antiporus gilbertit, Clk;

19) labium and Jabial palpi of Hyphydrus australis, Clk.; (20) Tabium and labial palpi of

Sternopriscus clavatus, Wehn.; (21) labium and labial palpi of Paroster insculptilis, Clk.

30 C. I, $. WATTS

Genus Sreynopriscus Sharp

Head with neck region not greatly narrower than the rest af the head.

Frontal projection with small notches and small teeth on yeutral margin of

upper quarter, otherwise smooth. Temporal spines very short. Labium tect-

angular, rounded at the tip. Siphon reduced to a slight bulge. Cerei lony

with mumerous setae,

The larvae of Sfernopriseus have strong affinities with the Hydroporini,

especially with the genera Neeterosona and Paroster, and appear to be

intermediate between these twa genera. The lateral projections are smaller

than those of Necteresoma and larger than those of Paroster, The temporal

spines are reduced in size from those found in Neeterosoma but ure not absent

as in Paroster,

Sternopriscus vlsvatus, Webi.

(Figs. 9, 15, 20)

Dorsal surface variegated light and dark brown, abdomen slightly darker

than rest of body, base of cerei and band about one-third of way along it pale.

Frontal projection and antenna as in Figs.

Length, 5-5-6-0 im. Head capsule +59 mim. wide, -94 mm. long.

Larvae have been collected from bare dams at Glenn Innes, New South

Wales, January 1961, and Adelaide, Octaber 196).

Genus Panosren Sharp

Head wide with no well-marked neck region. Frontal projection very

wide. notches small and narrow, small teeth on ventral margins of upper

guarter. Labtum slightly bi-lobed, labial palpi three-segmented, Sides of head

smooth with no temporal spines. Legs short, thick and covered with stout

setae, Siphon small, Jess than half the length of last sevrnent. Cerci long with

numerous setae.

The lack of temporal spines in Paroster is uniqne among the Wycdroporinii.

This feature, together with its small lateral projections and a wide neck are

characters that resemble or approach those in Biressus of the Bidessinii. The

three-segmented labial palpi is a character not found in other Hydroporinae;

although the palpi of many genera,, especially among the Hydroporimi, have a

constriction near the tap of the second joint which often gives the palpi the

appearance of being three-segmented.

Paroster insculptilis, Clk.

{Kigs, 21, 29, 8)

Dorsal surface light brown, middle abdominal segments a litle darker.

Ratio of length of siphom to length of rest of segment 1/3-3. Cerei long, 6-5

times the length of the last abdominal segment, Posterior edges of tergites witli

long setue.

Length, 4-4-4-S tom, Tead capsule -66 mm. wide, «92 mm. long.

Larvac were found in a grassy, temporary pool al Williamstown, South

Australia, October 1960 and September 1961,

Genus Cuosroxecres Sharp

Yead with neck region moderately developed, Frontal projection with

very wide deep notches, fine teeth ou the ventral margin of upper quarter and

ventral margin of lateral projectiuus and a pair of small spines on the ventral

LARVAE OF AUSTRALIAN DYSTICIDARN (COLEOPTERA ) 31

surface between the notch bases. Antennas and legs long, Siphun short and

sharp, about the same length as the rest of the segment. Cerci long, with

numerous long fine sétae,

Chostonectes latus Sharp.

(Fig, 6}

Dorsal surface variegated dark and light brown; frontal projection and ont-

line of temporal sutures pale. Lateral projections with outer edges roughly

parallel, blunt at the tips. ‘Two very small ventral spines on Jrontal projection,

separated by many times the width of their bases. Legs long and thin, claws

on front tarsi nearly eqnal and both long and thin.

Length, 6-5-7-0 mm. ead capsule last instar, -98 mm. wide, 1-5 mm.

long, Second instar, -55 sum. wide, -55 mana. long,

Numerous larvae collected from creeks in the Lower Ferntree Gully arca

of Melbourne, December 1961,

Chostonectes nebulosus McLeay.

(Figs. 5, 27)

_ Dorsal surface mottled dark and light brown, frontal projection and outline

of temporal sutures pale. Frontal projection thin, with a few small tecth on

ventral surface of upper third. Lateral projections thin, acutely pointed, with

their outer margins at 45° to each other, The two ventral spines are small and

are separated by twice the width of their bases. Legs long, claws on [ront tarsi

unequal, both long and thin,

Length, 5-3-5-7 mm. Head capsule, -73 mm. wide, 1:28 mm, long.

Two larvae were taken in February 196] from a dam at Collector, New

South Wales.

Chostonectes gigas Boh.

One larvae of this species was found ima weedy porid near Lower Ferntree

Gully, Melbourne, in December 1961, Unfortimately, the frontal projection of

the cxuyia was damaged. Froin what ean be seen the Jateral projections are

thicker and blunter than in C. nebulosus, wore or jess parallcl-sided and they

slope downwards to a greater devree than in the other species in the genus. The

spines are displaced in the specimen.

Length, LO mm. IRIcad capsule 1-15 mm. wide. 1-75 mm. long.

Genus Antirorvs Sharp

Ifeard narrow, neck not much narrower than rest of the head. Frontal pro-

jeclion with verv wide deep notches, fine teeth on ventral murgin of top quurter,

a pair of strong raised spincs on the veritral surface some distance below base

of notches. Legs long with numerous setae. Siphon vreatly reduced or absent.

Cerci Jong with numerous sctac,

The presence of spines on raised areas on the frontal projection is a distine-

tive feature of the genus. Other genera (Chostonectes, Macroporis) lave an

isolated pair of spines but these are much smaller and placed further forward

an the frontal projection. The size and relative position of these spincs are

useful taxonomic characters.

32 Cc. Ti. S. WATTS

Antiporus gilbertii, Clk.

(Pigs. 1, 18, 28)

Dorsal surface light brown, frontal projection and arca within temporal

sutures pale, large pale areas on rest of dorsal surface of head, cerci pale, Pair

of spines on frontal projection large and separated by four to eight times the

width of their bases, There are a few small teeth on the ventral side near the

bes of the frontal projection, Last abdominal segment not produced into a

siphon.

Length, 9-0-9-3 mm, Head capsule 1-01 mm. wide, 1-86 mm. long.

It is in this species that the spines on the frontal projection reach their maxi-

mum development,

Larvae collected fram a bare dam, Wilcannia, New South Wales, June 1961.

and a bare dam at Mt. Compass, South Australia, August 1961,

Antiporus femoralis Boh.

(Fig. 3)

Dorsal surface dark brown, frontal projection pale with pale strip extending

to temporal suture, rest of head and thorax with several pale patches, cerci with

basal half darker than apical, Pair of spines on frontal projection separated by

1-8 to 2 times the width of their bases. Numerous very small teeth on yentral

side of top half of frontal projection, Last abdominal segment produced into

a short siphon,

Length, 6-8-7-2 mm. Iead capsule, *89 mm,--94 mm. wide, 1°65 mm.-1+75

mim. long.

It is separated from A. vilbertit by its much darker colour, smaller size,

position of spines on the frontal projection and the presence of a short siphon,

Larvae collected from the deeper parts of a pool 30 miles south-west of

Canberra, January 1961; a weedy pool, Hobart, August 1961 (1st and 2nd

instars); and a moderately saline pool, Robe, August 1961 (numerous).

Antiporus blakei, Clk.

(fig. 2)

Dorsal surface a rich brown; frontal projection pale, with a pale strip

extending from this across the middle of the head and prothorax; sides of the

head also pale, the rest dark; basal portion of cerci dark, rest pale. Puir of

spines on frontal projection separated by twice the width of their bases. A

few small teeth near the tip on the ventral side of the frontal projection, Last

ubdominal segment produced inta a slight siphon.

Length, 5:8-6-5 mm. Head capsule, +78 mm.--$3 mm, wide, 1°58 mm.-1-61

mm. long.

It is readily separated from the other species by the conspicuous pale strip

on its dorsal surface, characters of the frontal projection and its slimmer shape

and smaller size.

Larvae collected from a weedy creek, Delorainc, Tasmania, January 1961;

a weedy creek (with algae Nitella sp.) Adelaide, April 1960.

LARVAE OF AUSTRALIAN DYSTICIDAK (COLEOPTERA ) 33

Genus NecrzrosomMa McLeay

Head with a narrow neck region. Frontal projection deeply notched, with

small teeth on ventral margin of upper quarter, and a pair of very small spines

on the ventral surface. Labium bi-lobed, Siphon short, about half the length

of the rest of the segment. Cerci long with numerous setae.

Prary 3

Figures 22-30. Line represents +1 mm. in all except Figs. 22 and 23, where it represents

Timm, (22) last abdominal segment and cerei of Lancetes lanceolatus, Clk.; (23) last

abdominal segment and cerci of Platynectes decumpunctatus, Fab.: (24) last abdominal

segment and cerci of Hyphydrus australis, Clk; (26) last abdominal segment and cerci of

Copelatus extensus, Sharp; (25) last abdominal segment of Macroporus gardnerii, Clk.;

(27) last abdominal segment of Chostonectes nebulosus McLeay; (28) last abdominal sezment

of Antiporus gilbertii, Clk.; (29) last abdominal segment of Paroster insculptilis, Clk.; (30)

last abdominal segment of Necterosoma penicillatus, Clk.

34 C. H. S, WATTS

Necterosoma dispar, Germ.

(Figs, 11, 17)

Necterosoma wollastoni, Clk.

Necterosoma penicillatus, Clk, = N. costipenni Lea.

(Figs. 30, 12, 16)

Dorsal surface brown, Head and thorax variegated light and dark brown.

Frontal projection with two very small spines on ventral side half way between

apex and notch bases, and placed nearer the margins than the centre. Ratio

of length of the siphon to the length of the rest of the segment is 1/2. Cerci

long, 23 times the length of siphon, basal portion 5-5 times the length of apical

portion.

Length, 6-S mm. Head capsule, +89--92 mm. wide, 1-24-1-28 mm, long.

This description applies to all three species which are very closely allied

and the differences hetween them very slight.

N, penicillatus differs from the other two species in the greater width of the

epistome, the basal angle of this sclerite being 90 deg., compared to 100 deg.

in the others. N. dispar has a very noticeable pale band on the cerei about one-

third of the way along it, this being Jess noticeable in N. penicillatus and nearly

absent in N. wollastoai. The pale areas on the head are well marked in N. peni-

cillatus. less so in N. dispar, and in N, wollastoni where the whole head is pale

except for the gutline of the temporal sutures.

N. wollastont Clk. collected from a tank near Wilevannia, north-vest New

South Wales.

N. dispar Germ, collected from mamerous dams and creeks near Adelaide.

N. penicillatus Clk. collected from numerous dams and crecks thronghout

New South Wales. Victoria, South Australia, Tasmania anc from southern

Queensland,

Genus Macroporus Sharp

Head wide, neck region relatively narrow. Frontal projection with deep,

wide notches, fine tecth on ventral margin of upper third and on the outer

ventral margins of the Iateral projections and a pair of spines on the ventral

surface between the notch buses. Labium short and weakly bifid. Siphon with

parallel sides, about twice the length of the rest of the segment. Cerci rela-

tively short with numerous sctae.

The siphon in this genus is larger and narrower than that of any other

known Hydroporinil, The nearest approach to it is Chostoneetes,

Macroporus gardnerit Clk,

(Figs. 4, 25)

Dorsal surface brown; frontal projection, areas of head and apical half of

eerei paler. Ventral surface of frontal projection smooth except for teeth as

for genns. Six to seyen teeth on ventral margin of lateral projection. The two

ventral spines fourteen times the width of their bases apart. Ratio of length

of siphou to length of rest of segment is 2-6/1.

Length, 10 mm-12 mm. Tead capsule 1-56 mm. wide and 2-25 mm, long.

Lurvae collected from a weedy creek (with algae Nitella sp.), Adelaide.

Septermber 1960.

LARVAE OF AUSTRALIAN DYSTICIDAE (COLEOPTERA ) 35

COLYMBETINAE

Genus PLatynectrrs Reg.

Head squarish with well-developed neck region. Temporal spines on a

line that will mect the ocelli. Mandibles about three times as long as wide.

Last segment of antenna less than half the length of the third segment. Labium

rather wide, maxillary stipes broad, about twice as long as wide, without hooks,

| Os

——_

Ny ra I 5 a

39 4Q # ae

Piatt 4

Figures 31-42. Line represents +] mm, (31) Maxilla of Copelatus extensus, Sharp;

(32) maxilla of Platynectes decumpunctatus, Fab.; (33) mandible of Platynectes decumpunc-

tatus, Fab., (34) dorsal view of partion of hind leg of P. decumpunctatus, Fab.; (35) antenna

of Lancetes lanceolatus, Clk,; (36) antenna of Rhantus pulverosus, Steph. (37) maxilla

of Homoeodytes scutelluris, Germ.; (38) front of clypeus of I. scutellaris; (39) labium of

H, scutellaris; (40) tip of antenna of Copelatus extensus Sharp; (41) maxilla of Rhantus

pulvernsus Steph.; (42) maxilla of Lancetes lanceolatus, Clk.

36 C. IL S&S. WATTS

Legs long, femora with spines on dorsal and ventral surfaces, tibia with several

scattered spines, und tarsi with a few spines at their apex. Last abdominal

seument not greatly produced backward between the cerci, Cerci short, with

a few long setae.

This venus appears to be closest to Iybius Erichsim from the northern

hemisphere from which it differs in having the Just abdaminal segment only a

little produced.

Plaiynectes decumpunctatus lab.

(Figs, 23, 33, 34, 32)

Colour variable, maxillary stipe as long as wide, bilobed at apex, the inner

Jobe carrying the galea, Legs thin; tibia with or without three spines on the

outer margin, with apical spines and a pair of spines on the inner edge near

apex; femora with spines along inver and outer margins. Cerci with setae near

the middle and an apical tuft of four svtac.

Variety 1. BReddish-brown. head and thoras variegated brown and. light

brown. Three spines on ontside of tibia.

Javiety 2. Dorsal surfaee dark brown, ventral surface light grey, head

+ i=} a 3

capsule wniturmly dark. ‘Tibia bare of spines, also fewer spines on the outside

of the femora than in var. 1.

Length, 10-12. mm. Head capsules last instar 1-58 mm, wide, 1°65 mm.

long, second instar. -99 mm, wide, 1-8 mm. Jong: first instar -73 mm, wide,

-§2 mim. lang,

Larvae collected from a weedy creek at Williamstown, South Australia,

October 1961 (var. 2): a weedy creek, Adclaide, December 1960 (var. 2);

Hackham, Sonth Australia (var. 1), October 1960; Mt. Compass, South Australia

(yar, 2), October 1960; 2 bare creek at Hobart (var. 1), August 1961; and a

saline pool at Robe, South Australia, Angust L961 (yar. 2).

P, decumpunctatus is a common, very variable and wide-spread species in

which the adults can he divided into [ow more or less distinct forms. The two

larval varieties described above differ markedly in their colouring, Only a very

few individuals that are intermediate between the two varicties as far as colour-

ing is concerned have been collected. The structural differences in the legs

appear to he constant. A few specimens from Mt. Compass agree with var. 1,

except that their setae are very much stouter. This difference is very nuticenble

and could indicate another variety. There is also a subtle difference in the

shape of the head and neck between the forms, var. 1 having the hind angle of

the head rounder and the neck more distinct than var. 2.

Genus Lanceres Sharp

Head squarish with a well-developed neck region, Temporal spines small

and on a line that will pass through the ocelli, Underside of head with a few

small spines. Maxillary stipe broad, with two hooks on anterior inner margin,

Antenna and palpi slender, last segment of antenna about half the length of the

third, Lees long with numerous fine spines and a row of very long setae on the

femora, tibia und tarsi, Cerci long: more than twice the length of the Inst

abdorinal sezment, and with many long setae, Main tracheal tubes narrow.

LARVAE OF AUSTRALIAN DYSTICIDAE (COLEOPTERA ) a7

Lancetes lanceolatus, Clk.

(Figs, 22, 42, 35)

Colour light brown; head with the clypeus, and a large patch in front of

each set of ocelli pale, the rest brown with numerous pale spots, Maxillary

stipes wide and flat, their palpi long and thin, the second and third joints nearly

eqnal in Jength and the first a bit longer, Labium broad, constricted in the

middle with two rows of very short spines along the anterior edge, Its. palpi

long and thin, the second joint being about two-thirds the length of the first.

Last abdominal segment cylindrical, truncate at apex. Cerci lang, three times

the length of the last abdominal segment.

Length, 15-16 mm. Head capsules, lust instar 2:53 mm, wide, 2-64 mm,

long; second instar 1-43 mm. wide, 1-66 mm, long.

The younger instars have rounder heads and longer appendages, especially

the more distal joints,

Larvae collected from a saline pool, Robe, Sonth Australia, August 1961;

Eudiumda, South Australia, August 1961; and Williamstown, South Australia,

September 1960.

Genus Turawros Lacord

Head squarish with wellamarked neck region, Temporal spines short and

strong. Underside of head with numerous short spines, Labim wide, maxillary

stipes broad, their inner margins curved. Last joint of the antenna large. more

then two-thirds the length of the third joint. legs with a moderate number of

spines which are mostly along the dorsal surface, a row of Jong setac on the

femora, libia and tarsi. Cerci short, aban? the leneth of the last abdominal

segment, with numerous setae. Main tracheal tubes wide.

Rhantus pulverosus, Steph.

(Figs, 36, +bL)

Compact, brown, upper surface variegated light and dark brown. Head

square with numerous small spines on the underside which are arranged in four

patches, the two largest near the base of the head on either side of the gulga and

a smaller patch on each side of the head midway along the outer margins,

There is also a Jine of spines running obliquely between the basal and lateral

patches on each side of the head. The last abdominal seement is slightly less

thim twice the length of the second tu last segment, The cerci are slightly

longer than the last abdominal segment, and have about twenty-five setae on

their inner sides.

Length. 17-19 mm, Head capsules, last instar 2-30 mm. wide, 2:57 mm.

Jong, second instar 1-38 mm. wide, |-47 min, long.

There are two rows of light-coloured spots arranged in two whorls in the

centre of the head, This same pattern accars in Lancetes lancealatus and iu

several other species, The arrangement of the spines on the underside of the

head appears to be constant im this species.

Larvae collected from a sheep trough, Sheffield, Tasmania, January 1960;

Williarmstown, South Australia, October 1960; Canberra, January 1961.

3 C, H. 5. WATTS

Genus Coprnatus Er.

Head with neck region well developed. Temporal spines strong. Labium

wide, labial palpi very short, Maxillary stipe broad with two to three large

hooks on their inner anterior margin. Maxillary palpi and antennae short.

Last segment of antennae biramous, Mandibles with fine tecth on inner edge.

Legs stout with a few spines. Cerci yery short, less than the length of the

last abdominal segment. Body covered with small, round, raised areas. Ter-

ites with numerous short, strong spines, especially along the posterior margins,

The larvae of Copelutus have many characters not found in any other

Colymbetinac; their bodies tend to be harder, more cylindrical, and to have

more and much stronger spines especially aloug the posterior margins of the

tergites; they have a biramous last joint to their antennae although the extra

portion is often small and inconspicuous; their cerci are smaller and stouter than

in other members of the group; their labial palpi are small and stout, whereas

the rest of the group have rather long palpi; and their mandibles are toothed.

This last character is no doubt correlated with the fact that these larvac

swallow. their food whereas in all other Dytiscids digestion is purtly external

and feeding is done by sucking the digested body conteuts of the prey into the

mouth through a partially closed groove in the mandibles, This method. of

feeding was first noticed by Williams, in the Hawaiian species C. parvulys, and

has since been observed in all five Australian species that I have seen, Larvae

of C, extensus have been observed in the field to swallow Chironomid larvae as

long as themselves, the process taking about five minutes, With Daphnia as

prey, GC, extensys crushes the crustacean up against its mouth, holding it there

with ats mandibles. 1t then sucks the bady contents of the Daphunin into its

mauth,

Copelatus cxtensus, Sharp

(Figs, 26, 40, 31)

Uniformly dark brown. Tergites covered with numerous staut spines on

raised areas, their posterior margins with siout blunt spines rather irreularly

spaced but averaging about the width of their bases apart. Maxillary stipes with

three books, galea greatly elongated and curved. Apical segment of antennae

small and yentyally placed. Cerci short: 0-4 times the length of the last

ahdominal segment, with a few fine setae.

Length, 12-13 mm, Head capsules. last instar 1-$8 mim. wide, 1-S4 mm.

long, seeand instar 1-31 mm, wide, 1-3! mm, lony.

The hody spines are well developed in this species as is the peculiar warting

of the body surface. Larvae that I take to be those of C. nigritulus Ship, but

have not bred, greatly resemble those wf C, extensus.

Larvae collected from the muddy bottom of a shallow tank, Mt Lofty,

South Australia, August 1960, and January 1961.

CYBISTRINAE

Genus Howovonvres Reg.

Head anteriorly tri-lobed, middle lobe narrow and separated from lateral

lobes by deep clefts, the lateral lobes wide and strongly dentate along their

unterior margins. Antennae and maxillary palpi with nine segroents, Jabial

palpi with four, last segment of antennae hiramous, Liga very small, Cerci

rudimentary.

LARVAE OF AUSTRALIAN DYSTICIDAE (COLEOPTERA ) 39

Differs from Cybhister in the greatly reduced ligula and in having the lobes

on the head strongly dentale, each touth with a dense tuft of short setae at

its tip,

Homocodytes soutellaris, Germ.

(Figs. 37, 38, 39)

Body grey-brown, head and thorax reddish-brown, black stripes on either

side of the hody being especially noticeable on the thorax, ‘Teeth on front of

head. variable in number (thirteen to eighteen) often asymmetrically arranged.

Last two abdominal segments with fringe of long setae, rest of body sparsely

coyered with long setae. There are two chitinous knobs in the middle of the

dorsal side of the head. Cerci small and vestidual, placed about three times

their length back from the tip of the last abdominal segment.

Length, 45-55 mm. Head capsules, Iast instar 6-1 mm. wide, 5-0 mm.

long, second instar 3:8 mm, wide, 4-0 mm, long, first instar 2-4 mm. wide, 2-5

mim. long.

The younger instars are smaller and lack the black stripes on the thorax

and the chitinous knobs on the head are more noticeable.

Larvae collected from a weedy creek, Canberra, January [961; a weedy pool,

Melbourne, December 1961; Lake Baga, Victoria, January L961; and a swamp,

Manmum, South Australia, September 1961.

APPENDIX

The following genera are all represented in Australia by species whose

larvae [ have not s¢en. But larvae of certain non-Australian species have been

described and the following diagnosis (modified after Bertraud, 19238) are

based on these deseriptions.

Genus Laccornitus Leach

Larvae without frontal projection and without swimming hairs. Body

elongate, legs long and slender, Sides of head, in older larvae, with only a

few long strong spines (three-five).

Distribution in Australia; Queensland, Northern T. ercitory, north-west Aus-

tralia, northern Tasmania and southern Victoria.

Genus Ereres Laporte

Larvae without frontal projection. Last few abdominal segments provided

with a lateral fringe of swimming hairs, Body elongated and humped. Clypeus

coniplete, cerci without swimming hairs, Ligula small with four spines.

Distribution in Australia: throughout the inland areas.

Genus Raaxtancus Sharp

Larvae without frontal projection, last abdominal segments provided with

a lateral fringe of swimming hairs. Body elongate, clypeus complete. Cerci

without swimming hairs. Ligula simple, yery long, nearly the length of the

first joint of the labial palpi. with six spines.

Distribution in Australia; Qucenslind and Northern Territary.

40 C. H. S. WATTS

Genus Hypaticus Leach

Larvae without frontal projection. Last few abdominal segments with

lateral fringes of swimming hairs. Body clongate, not humped. Clypeus com-

plete, cerci without swimming hairs. Ligula small, bilobed.

Distribution in Australia: Queensland, Northern Territory, South Australia

(River Murray), and New South Wales.

Genus CyYsIsTER Curt.

Larvae without frontal projection. Last few abdominal segments with

lateral fringe of swimming hairs. Body elongate, not humped. Clypeus divided

into three lohes, lateral lobes not, or only slightly, dentate. Ligula simple, of

moderate length, Cerci rudimentary.

Distribution in Australia: Queensland, Northern Territory, north-west

Australia, New South Wales and South Australia.

Genus Hyproyarus Motsch.

Larvae witli frontal projection. Body squat, very short and depressed; head

with a long frontal projection which is slightly notched. Cerci very short

(shorter than last abdominal segment in last instar). Siphon elongate. Labium

short and subtriangular,

Distribution in Australia: Queensland, Northern Territory, New South Wales,

Victoria and South Australia,

REFERENCES

Brerrrann, H., 1928. Les larves des Dytiscides, Hydrobiides, Haliplides. TEnevel. ent. (A),

10, VI, 366 pp.

SHanv, D,, 1882. On Aquatic Carnivorous Coleoptera or Dytiscidue. Sci. trans. Royal

Dublin Soe., V, 2, Series 2.

Witurams, F. X., 1936. Biological studics m Hawaiian water-loving insects. Part 8.

Coleoptera or beetles. Proe, Hawaii, Ent, Soc, (1935), 9, pp. 235-273.

Bovine, A. G., and Craicuesn, F. C., 1930. An illustrated synopsis of the principal larval

forms of the Order Coleopter. Ent. Amer., 11 (n.s.), V-: 1-80, (2) 81-160, (Re-

printed 1953.)

Leacu, H. B., and Cuanprier, I. P., 1956. Aquatic Coleoptera in Aquatic insects of Cali-

fornia. Ed. R. Usinger, Univ. California Press. 1956.

SOME GEOMORPHOLOGICAL PROBLEMS OF THE

NULLARBOR PLAIN

BY J. N. JENNINGS

Summary

On the basis of further data provided by recent speleological parties, some of the geomorphological

problems of the Nullarbor are rediscussed. The extremely flat surface of the Plain is regarded

neither as a planation surface nor as a stripped structural surface but as an almost unmodified

emerged sedimentary surf ace. Faulting along the coastline and the Harnpton Range remains

unproven; the morphology is readily explicable in terms of costal erosion and subaerial weathering

during the substantial Pleistocene-Recent changes in relative level of land and sea of which there is

stratigraphical evidence. The shallow caves are primarily of vadose origin but are localised and still

much influenced in their character by a zone of small-scale phreatic preparation of unusual

intensity. The few deep caves die not considered to be phreatic in the proper sense of that term, but

have developed along the lines of Glennie’s theory of “master caves”. They are unusually large

caves for their lithological context and their coastal distribution is thought to be climatic in origin,

rather than structural. King's views that cave destruction, rather than formation, is in progress today

and that Pleistocene pluvials were important for the development of the Nullarbor caves, are

supported. Nevertheless, changing relative level of land and sea is also thought to have been

important in that it shifted the watertable and the level of phreatic solution. Although our

knowledge remains small, on the whole it points to poverty, rather than richness, in caves in the

Nullarbor and the underground as well as the surface morphology is indicative of a retarded,

immature karst. This is thought to indicate that Pleistocene pluvials did not cause the climate to

depart very much or very long from its present semi-arid to arid range.

SOME GROMORPHOLOGICAL PROBLEMS OF THE

NULLARBOR PLAIN

by J. N. Jenninés®

(Communicated by Dr. N. H. Ludbrook)

[Read 9 Aigust 1962]

SUMMARY

On the basis of further data provided by recent speleologiaal parties,

some of the geomorphological problems of the Nullarbor are reciseussed,

The estremely fat surface of the Plain is regiurded neither as a planation

surfuce nor as a stripped structural surface but as an almost unmodified emerpced

sedimentary surface, Faulting along the coastline and the Hasypton Range

remains unproven: the morplialagy is readily expleable in terus af coastil

erosion amd subaerial weathering duriug the substantial Vleistacenc-Reeent

changes in relative level of lwnd and sea of which there is stratigeaphical

vvidence.

The shallow Gives are primarily of vadose origin Wut are localised anu still

much inflnénced in their character by a zone of smialescale phrewtico preparation

of unusual intensity,

The few decp caves are not considered la be phrealie in the proper sense

of that term, but have developed along the lines of Glennie’s theary of “master

faves”. They arc unusually hie caves for their lithological context and their

couslal disteifmtion is thanght to be climatic in origin, rather than structural.

King’s wews that cave destruction, rather than formution, is i pragress

today ancl that Pleistocene pluyials were important for the development of the

Nullarbor caves, aré supported. Nevertheless, changing relative Tevet of land

ancl sea is also thought to have been importimt in that it shifted the water-

table and the level of phreatie sohitian.

Although our knowledye remains small, on the whole it pointy to poverty,

vather than richuess, in Gives in the Nullarbor and the underground as well as

the surface morphology is indicative of a celarded, immature karst. This is

thowght to indicate that Pleistoeene pinvials did not cause the climate to depart

very much or yery long from its present semi-arid to arid rauge.

INTRODUCTION

Despite its simplicity of surface form, the Nullarbor Plain is of considerable

interest as one of the world’s largest karst regions, though as might be expected

a good deal of that interest centtes on the underground geomorphology. Inci-

dental observations relevant to this therae are to be found in many of the carly

accounts of explorers and geologists but the first man to organise expeditions

specifically in this connection was Captain J. M. Thomson from 1934 onwards.

This long-continued effort culminated in his own and D. King’s papers in this

journal (Thomson, 1950; King, 1950) though he has led parties into the Nullarbor

since then. In 1957 the Cave Exploration Group of South Australia organised

an expedition to the Plain for the newly-founded Australian Speleological

Federation, Over 60. members of the many cxving societies which had sprung

up in Australia since the war. participated in varied scientific work as well as

* Research School of Pacific Studies, Australian National University.

Trans, Ray. Soc. 8, Aust. (1963), Vol. 87,

J]. N. JENNINGS

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CEOMORPHOLOGICAL PROBLEMS, NULLARBOR PLAIN a3

straightforward cave exploration. Three other parties have added to this kunw-

leclwe sinee then.

The geomorphological report of the 1957 expedition, prepared by the wrilve,

was first made available privately to subsequent expeditions and later given wider

cireulation by CEGSA (Jennings, 1961). Attention is centred in this paper cy

certain problems of interpretation, ‘Though the yiews expressed differ significantly

ut certain points from those of King, it is not maintained that they. approach

definitiveness and conclusively displace earlier ideas. Our knowledge of the

Nullarbor Plain remains very inadeqnate. Nevertheless, this account is based

on much more detailed cave survey than was previously available. Many cavers

are responsible but R, T. Sexton must be singled out for acknowledgment in this

regard, not only for his own contribution but for the informed stimulus he has

viven to others. Opportunity is taken to illustrate this paper with previously

unpublished or revised cave surveys.*

WHAT SORT OF GEOMOKPLIOLOGICAL SURFACK DOKS

TUE PLAIN COMPRISE?

Tf the name is taken to connote not solely the treeless plains to whith it

strictly applies, but also the topographically similar vet serub-covered extensions

ever the same Terthury limestone, the Nullarbor forms one of the most exten-

sively and uniformly plane bedrock surfaces of the world (Fig. 1). Yet its

gencrie nuture has su far occasioned litte: discussion.

The levelness of the Plain has always astonished travellers from Eyre onwards,

Traversing its inner margin for the first time, Giles comments, “A hieyele could

he ridden, | believe, over the whole extent of the plain”. The uniformity uf the

relief could not be revealed more clearly than by the course of the Transeon-

tinental Ruilway including as it does one absolutely straight reach of 300 miles.

The only widespread diversification of the surface is so minor that it edvuld

almost be termed “mierv-relief”, This consists af gentle undulations of an

amplitude of about 10 feet and a wavelength of several miles. In some areas the

local relief is rather greater than this but was never formd to be more than

25-30 feet. Examination of a wartime run of trimetrogen air photographs along

the coust supports Woolnough (1933) rather than ‘Tate (1879) in the question of

the presence or absence of structural control, Since the undulations are arranged

alung two trencls at right angles to one another NE-SW and NW-SE — and tris

seems on the ground to be the joint pattern of the Nullarbor Limestone, it is

reasimuble to attribute the features to differential solution.

There are also a very few shallaw valleys. Only one of these, close to

Koonalde homestead, was examined in the field for four miles though its Fall

length is greater, Its Hat floor, 15-20 feet below the Plain. has a continuous down

eradient seuwards, Though ventle aid with only an occasional rock outcrop,

its sides define it well and a similar slope cuts it olf before it reaches the coast.

turning it into a blind valley, Prom a northern part of the Plain, Jones (1880)

writes of valleys 30 and 60 feet deep, but how continuous these are is not clear

sine Le also writes of “valleys invariably broken by cross-ridges”. Though there

was no stream bed to be seen in the Kounulda example, valleys such as it must

have been the product of concentrated minolk.

M I, N. JENNINGS

More mamecrous than the valleys but still infrequent in relation to the ares

involved are “circular hollows” (Jones, 1880.) or “dongas” (Gibson, 1909). ‘These

are smaller, more cirenlar and better defined than the tronubs of the undulations

previously described, Tliey cormmonly range from 50-60 feet to over 400 Vurds

acrass and lie 10-20 feet helow the Plain with lat foors which may be penctrated

hy blowholes. Bedrock onterops rarely an their flanks, which are not very

steeply inclined. These hive heen interpreted ss solution dolines previously

(Jennings, 1961), Even though the writer would not accept the generalisation

by Coleman and Balchin (1959) that all dolines are of collapse origin, it must be

adiilted the Nullarbor “circular hollows” could have been derived from collapse

Uolines by degradation of their sides. Because of the stall depth of the “circular

hollows", only shallow caves would be inyolved if they are of collapse orluin.

Size is not a problem when the dimensions of shallow caves such as Jimmy's

Cive N23° (Pig, 5) are borne ii mind but shape is since the caves tend to an

elongution not characteristic of the dolines under discussion.

Less frequent but unmistakeable in origin are the collapse dolines. These

ohieng or circuku enclosed depressions are srrounded on all or most sides by

vertical clifly or steep broken rock slopes; they are deeper in relation to their

urea than the “circular hollows”. The collapse doling of Murranwijinie Cave N7,

15-25 feet deep, is roughly trapezoidal in shape through joint control, 120 feet

long und 35 feet across. Knowles Caye N22 is a cave remnant at the end of

un elongated collapse doling, 15-30 feet deep, 60 feet avross and 320 feet long,

With no known cave development from it, Chowilla Landslip N17 is one of the

largest collapse dolines, about 00 feet deep and ronghly elliptical in plan, approxi-

mately 150 feet by 200 feel. The eutrauce valloy to Abrakurric Cave N3 is

much larger still, being over 700 feet long and 200 feet across, but its floor falls

gradually from 10 feet depth to nearly 100 feet at the cave entrance, So it

partakes more af the nature of a blind valley; it may have begun as a collapse

doline and have been extended later by spring sapping northwards,

All these kurst features are few and far between; the Plain is in fact an

ineredibly featureless low plateau, rising imperceptibly to the eye tram heights

of 150-250 feet on the coust to 450-650 teet on its inland margin. This rise is

compounded of a S-N element and an E-W one. Some canses of this lack of

relief are abvious,

(a) There was virtttally no initial tectonic relief. Possible exceptinns to this

we the escarpment of the Hampton Range to be discussed below and alsa three

low scarps westward of Ooldea (Jones, 1880), which may be due to faulting.

The rocks are almost horizantal: Ladhrook has suggested a slight southward and

easQward tilting in accardanee with the present relief. :

(b) Nor has there been sufficient surface drainage to generate erosional

topography of Huviatile origin, the purity of the limestones has virtually elimin-

ited this factor,

(¢) Moreaver, the low annual rainfall of 12 to 5 inches has ensured that

karsl development has not proceeded Far enough to diversify the surface in

its Hwn peculiar manner to viny marked devree.

(dl) Though it has been maintained that deflation of the culeareons desert

soils of the Nullarbor has provided the materials for soils aronnd the Lake Eyre

Tegion (Jessup. 1961; Stephens. 1961), the quantities involved do not bulk large

in relation to the extent of the Flin.

"The eaves of mauny Australlan lirnoestene areas have been indexeil: the Nullarhor caus

have the letter prefix N Jullowed by numbers,

GEOMORPHOLOGICAL PROBLEMS, NULLARBOR PLAIN 15

What sort of surfice then is represented here? That it is not a planatthin

surfice due to any form of crosion whatever seems to be substantiated by the

upparent oceurrence over the whole surface of the Plain of a style und thin

formation, thy Lower Miocene Nullurbor Limestone (Luin in Glaessner

and Parkin, 1955). At Pidinga its margin has been chatered back some little

way (King, 1951) and north of Watson, Ludbrook (1961) indicates the possi-

hility of same removal of Nullarbor Limestone again at the margin of the Plain.

Within its vast extent, however, the Nullarbor Limestone outcrops everywhere

as far as is known and if erosional phination were involved, older formations

would surely be found over substantial areas, On the other hand, if it wore a

stripped structural surface, reronants of vounger sedimentary covers would

survive here and there and such have not yet come to light, Rather does the

Plain appear to be the original sedimentary surface of Miocene ave raised above

scei-level, tilted slightly downward ty the south and east in the process and

preserved qlroost womodified since, The useful term “sediplain® has been pre-

posed by R, O. Bronuscloweiler for this kind of surface, though to the writer's

knowledeu he hay not applied the idea nor the term to this case

This conclusion is relevant to the theory of karst erosion cvcles since many

unthoarities have taken the view that the initial stage in the evolution of a dotine

karst sviely as this must include the development of a surface valley system by

runote Llere the dolines, modest thouch they are in pumbers, have been pro-

howd withawt sueh prior development of valleys. This initial stage has Lew

hded beeanse of the absence of any significant cover ef later imperviens reks

river the Nalhirbor Limestone

WHA'T [IS THE NATURE OF THE NULLARBOR COASTLINE?

Such long reaches of unbroken cliffs as constitute much of the coast uf the

Nullarbor Plain ave rare in the world (Valentin, 1952) and it is litle wouder tat

thev aronsed speoulation from Flinders onwards. He postulated an inland valley

parallel to the coast to expluin the absence of any valleys interrupting the even

crostline of the Bitida clifls between Kucla and the Head of the Bight, However,

Eyre showed there was uo such valley. Since then the contimmity and linearity

af the cliffs has prompted geologists from time to tine to postuluke a fanlt ortin

for them (eg, Woodward, 1890; Woolncugh, 1933; David, ed, Browne, 1950),

However, the danger of postulating faults sulely on physiographic grounds is a

wellknown one and here there ore perhaps optimal conditions for a regular

cliffline without such a direct tectonie origin, "The same combinations of almnst

horizontal pure limestones in a semi-arid tg) arid climate which accounts far

the uniformity of the Plain also provides the waves with a uniform height of

uniform rock on which to work,

Not all the coastline is clifled. At the [lead of the Bight, the Bindu elilfs

puss iland wad are buried wider dunes, At their other extremity at Muela they

merge into the searp which has been called tue Tlampten Range aud which forms

the inner houndary of the Roe Plain, a coastal lowland up to 25 miles wide, Be-

vend Kyre the coastal clills reappear even higher than in the Benda cliffs and

persist to beyond Point Culver, Once more the clitls are transformed into a

scarp behind w narrow coastal lowland extending to Israelite Bay, a remote

area from which no scientific observalions seem to have been gathered,

The Hampton Range and the Roe Plain provide the best appartunity for

proving or disproving faulting along the coust. Frost (1958) Jas made the most

recent case for considering the rclicf bore as truly tectonic, But his evidence

of jointing from the Roe Plain is too meagre for his arguraent from joint pattertis

46 J. N. JENNINGS

of the area to be very convincing. Otherwise he depends on the lithological

correlation of Madura No, 1 bore at the foot of the scarp with the bores on the

plateau to the north. He maintains that the Nullarbor Limestone underlies the

Roe Plain, thrown down 300 feet along the line of the scarp. Examining the

same bores palaeontologically. Ludbrook (1958) came to the opposite view that

COASTAL PROFILES

NULLARBOR PLAIN

Nullarbor Limestone Foo

Mifson’s Blut oose

Limestone wos 8

Modern hf freshly cut.

Unconsolidated

| seyK Blown Sand

Pleistocene Cliff SEE Consolidated Blown Sand

and Aeolianite

Breccia

7wo-cyctle HF e.g. Ol Pleistocene chi hurried by Pleistocene

Wilson's BlvT?. Based on fate. dunes eg. Head of Bight, Based on Fate.

Hampton Range

Degraded

Pleistocene Cliff

Beer SS ae

Pleistocene

reoeosces

GEGMORPHOLOGICAL PROBLEMS, NULLARBOR PLAIN 17

the Nullarbor Limestone has been remoyed by marine erosion and that it ts the

Eocene Wilson Blut Limestone which underlies the coastal lowland. Unfortun-

ately this divergence of interpretation depends on one surmmple since the Madura

bore was sampled once only between 30 and 500 feet.?

Further styatigraphical evidence may be necessary before this issne can be

finally decided; one thing seems certain, however, namely, that the Iampton

Range has been subjected toy marine erosion and is no longer a simple fault scarp.

Air photographs show that the western part of the Hampton Range takes the

form of a series vf shallow. smooth curves i plan, best interpreted as the wave-

cut hays of a former sea clifl The varying vertical profiles support the same

interpretation (Fig. 2). On the Hampton Range only the Nullarbor Limestone

presents a free face; the Wilson Bhiff Limestone below has a much less steep,

though fairly constant slope, partly soil and rubble covered, At Wilson Bluff

sell modern wave attack has fashioned a fresh cliff at the base of this incline

in the weaker limestone, This composite profile is buried by the Merdayerrali

Sardpatch but reappears to the east where the lower cliff grows in height grada-

ally to eliminate the intervening bevel, ‘Thus the typical vertical to overhanging

profile of the Bunda cliffs is achieved, with the slight bulge of the overlying

more resistant Nullarbor Limestone, Af the far end of this cliffline the reverse

succession is found, the bevel gradually reappearing before the dunes at the

Heid of the Bight bury everything, "The bevelled cliffine has the appearance

of a “two-cycle” clifE (Cotton, 1951), slightly complicated by the different resist-

unce to erosion of the two limestones,

It is inferred then that during a former higher stand in the relative level of

land ancl sea, the Whole coast was clifted; during a subsequent phase of lowered

sea-level this cliff was degraded by subverial weathering to produce the profile

of the Hamnptouw Rane, which reflects the different responses of the two lime-

ytunes, Since then wave action has destroyed this degraded cliffline wlony the

Bunda cliffs. At the Head of the Bight, and near Eucla, the bevel in the Wilsen

Bliat Limestone is still being removed and the “two-cvele” profile persists tem-

povarily. The sea caves well above sea-level near Twilight Cove, reported by

Gilson (1909), probably relate ta another event in the history of the relutive

level of Jand and sea in the region.

There is, of conrse, stratizraphical evidence for move than one high stand

af sea-level relative to the Jind. Lidbrook (1955) reports Pleistocene shelly

limestone of marine origin wt + SO-1L02 fear in Macuta No. 1 bore; similar

lunestone his been collected from the cave six miles south of Madura on the

Boe Plain, of unlmnewn hefeht bnt at least — 635 feet (Ladhroak, pers. cari. ),

There is also Pleistocene marine culeareans sandstone at +120 feet from. the

easteco cnd of the Plain (Ladhrook, in Clacssner and Parkin, 1958). All these

could relate to the same phase on present knowledge. However, it is much less

likely Uhat the marine cileareous sandstone at + 12 teet at the eastern end ot

Roe Plain and the emerged sliell beds at 4- 6 feet al Yalata Swamp near the Llead

of the Bight, both reported by Tate (1879) as having « Recent fauna, belong th

this stand, rather than to a later one.

Tate also noted! that Pleistocene aeolian calvarenite was plastered agalnst in

old cliffline al the Head of the Bight, at Merdayerrah and at Fucla, We moain-

tained that this dune limestone extends below sea-level and implies a stand at

sealeyel below the present. Ludbrook (pers. comm.) confirms this with the

imormation that the Twin Rocks, sea stacks newr the Head of the Bight, are alsa

a Hecent unpublished work by Ludbrook on Eyre No. 1 Oihwell, 15 miles soul «at

Maduea. confirnns the absence af Nullarbor Limestone finn the Roe Phin.

AS J. N. JENNINGS

formed of this rock. Taking Tate’s figure illustrating the relationship of the

aeolian calcarenite to the old cliff literally, it must be inferred that the dunes

were built up: before the old cliff had been degraded by subacrial weathering.

A tentative sequence of these coastal events could be put together, but in

view of the known complexity of sea-level changes elsewhere and the present

meagre information from the region itself, there is no great advantage in doing

this as yet. That there have been substantial changes in the relative level of

land aud sea in the area must, however, be noted because of its relevance ta

later discussion.

ARE THE SHALLOW CAVES VADOSE OR PHREATIC?

Thomson (1950) divided the caves of the Plain into a twofold scheme of

shallow and deep; this was followed by King (1950) in interpreting their de-

velopment, Further knowledge scems to underline this dichotomy as significant,

though there ave caves intermediate in level, e.g. the cave leading east from

the Weebubbie doling, and lying between 60 and 120 feet below the Plain.

Reaching to depths between 15 und 80 feet, the shallow caves are con-

fined to the Nullarbor Limestone, generally a hard, dense, well-jointed, ervstal-

line limestone, grey or cream in colour, Usually small with one to two hundred

lofMID)

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Fig. 3. Scheme of evoluiton of shallow caves,

GEOMORPIIOLOGICAL PROBLEMS, NULLARBOR PLAIN 49

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feet of passaue, the shallow caves are knawn also to include quite large chambers

and up to 600-700 feet of passages. They are widely distributed through the

Plain, at least south of the Transcontinental Railway.

Thomson associates particular kinds of entrance with particular forms of

shallow cave, but the relationships are more complex than that (Fig. 3). Four

types of entrance haye been observed by the writer:

(a) Vertical shafts or wells, roughly circular in cross-section, 2-4 feet in

diameter and up to 15-20 feet deep, eg. New Cave N11, Their surfaces are

commonly marked by conchoidal hollowings, which may be attributed to turbu-

lent water under gravity dissolving and possibly also abrading the rock. These

are the typical “blowholes” of the Plain.

(b) Roof collapse windows. Enlargement of the chambers below can also

lead to enlargement of the shafts by fracture along joint planes, e.g, White Wells

Cave N14.

The Catacombs N20.

30 J. N. JENNINGS

(d) Large Jateral entries in the sides of dolines, Extensive roof collapse

mtv result in a steep-walled doline with wide enteies at the base of the cliff rim

leading into the remainder of the cave, e.g. Murrawijinie Cave N7.

The vertical solution shafts lead dow iolo several types of cave, Simplest

uf all is the single bottle-shaped chamber, Thomson's “hottle-neck cave’. Fig. 4

vhows N32 Pothole neur Kounalda homestead, which fills into this category

of cave though the entrauce shaft is not a simple une, Other shafts lead into

complex arrangements of small passages, e.g, N19 Gave close tu Weebubbie;

much of this complexity is due to rock collapse. whiell is characteristic of even

very small shallow caves. The shaft type of entry may still survive water large,

Hat-roofed chambers have developed, frany which small passages branch off

horizontally or downwurds, muybe leading to smaller chambers at lower levels,

ww New Cave NU. More usually the development of these large chambers

vlase below the surface results in entrances oF the second and third types being

prodyved, Kventually collapse destroys most of such chambers and the renmants

around the rim of the collapse doline have much more of the nature of cock

shelters thar) of Hite caves, Ga. Knowles Cave N22,

King (1950) hus argued that the shallow caves are of vadose origin, chiefly

hiccause they have # steep gradient, especially tv the vertical shafts and becuse

they possess dripstone decorations. The latter point is in mo vay conclusive

since dripstone and flawstone feates can form in caves of diverse genesis snb-

sequent to them excavation. In fact, in comparison with the eaves of most

wtber parts of Australia known to the writer they are very poor in calcite decora-

tions; by contrast wypsum flowers seem more frequent than elsewhere.

It is true, nevertheless, that the vertical shafts exhibit evorsional sculpturmg

ty be associated with descending vadose water, Moreover, not only are parts

mf the cave Goors fairly level with water-laid accumulations of loamy earth, sill

wid rock debris, but intermittent watercourses af silt and angular gravel can

he seen descending to lower levels through irregular masses af rock fall. No

erosional channels in solid rock have yet been seen in the shallow caves though

u-catige will be mentioned later which casts no doubt on the view that vadose

action has been very important in the fashioning af the shallow caves.

Nevertheless, many of the shallow caves, o.g. Jimmy's Cave N23 (Mig, 3),

show pronounced horizontal deyclopment just below a massive surkiee erust

of 10-30 feet thickness and in a zone of intense perforation by solution (nbes

a few inches in diameter. Not only do walls of chambers and passages show

whastomosing networks of small halftubes in exposed bedding- and joint-planes,

but irregular fallen blocks show that the whole mass of the rock is penetruted in

all directions by these tubes. In parts of White Wells Gave N14 the tubes

lave heen filled with dark-coloured calcite and stand ont clearly (Pl 1). This

zone ut perforation can be seen excellently in the coastil cliffs south of Koonalda

where itis seen to be couhned to the Nullarbor Limestone.

Sueli anastomosing solution tubes have geverally been regarded hy British

and American speleologists as due to true phreatic solution, ie. by slowly eir-

eilating water beneath aw wetertable (Bretz, 1942; Clennie, 1954). But they

ive usually deseribed as restrieted to joint- anc bedding-planes: here there is no

such restriction. This intense zone of phreatie preparation has nat only localised

the level of developmient of the shallow caves, it is responsible alsa lor the

prevalence of eave breakdown in them and for the typical irregularity of walls

and floors. The flat roofs are often a reflection of the unperforated surface laver

of Limestone. The lack of bedrock erosional channels can alyo be attributed tu

GEOMORPHOLOGICAL PROBLEMS, NULLARBOR PLAIN ol

this weakening of the limestone, Breakdown due to the weakness of the riddled

limestone is apparently still quite active today; Thomson has reported collapse

in The Catacombs N20 and in Ivy Cave N13 between visits separated by only

a few years.

Caves are not usually dae ta one phase of excavation only, be it vadose

or phreutic: indeed nearly all caves must begin by something closely akin to

phreatic solution. The problem is to assess the relative importance of the dif-

ferent phases in producing the present morphology. It is clear that an early

phase of intense, small-scale phreatic preparation has remained important in

governing the character of the present-day shallow caves of the Plain,

JIMMY'S CAVE N 23

GRADE2 SKETCH, 14:1:1957 BY J.N, JENNINGS

fiat sendy

fleor

dow

ridenston hy

Highest rage 7

aw,

ons dere «St t °

Nf clemd owe ‘ fo

a Pe fare a

Le ,

Vbvere denevsstan

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Sr SS eat

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—~————_<

Vig. 5. Jimmy’s Caw N33.

ARE THE DEEP CAVES PHREATIC?

The known deep caves of the Nullarbor — from west to east, Cocklebiddy,

Abrakutrie N3, Wecbubbie N2, Warhla Nl, Koonalda N4 — have entrances

leading from the bottoms of callapse dolines at 80-100 fect down, except for

Abrakurrie into which the blind valley already mentioned leads at 90-100 feet

helow the Plain. As a result they are almost entirely developed in the Wilson

Bluff Limestone of Upper Eocene age. This pnte bryozoal ecalcarenite is friable

und chalky, though somewhat harder than a typical chalk; joints arc few, but

King reports it to have a porosity of 26 p.c, The deep caves are substantial in

size (Figs. 6 and 7; Pls. 2 and 3) and are therefore of interest in this lithological

context since until very receutly only very small caves have been found in the

Cretaceous Chalk of N.W. Europe and the longer caves found Jatterly apparently

do not possess the large dimensions in other directions of the Nullarbor examples,

52 J. N. JENNINGS

From the entrances, steep slopes lead down to levels of 150-300 feet below

the Plain where fairly horizontal levels are found made up of large halls, 40-60

feet high and 80-120 feet wide, Warbla is the shortest in length with 800 feet

and Koonalda the longest with an overall length of 2,700 feet, together with

another 1,000 feet in branches. However, these Jengths are a much less. satis-

factory indication of their size than their floor area or, even better, their yolume

would be. Indeed, they are very impressive caves because of their bold, spacious,

simple forms — flat roofs, smoothly arching walls and apse-like ends — and be-

WEEBUBBIE CAVE N2

100 an BOOFh

Selected sowadiags in feet Mae

Surveyed ¢ &7. Sexton &

Pury, Jan JIse.

Lake resurveped by / 8 Hte-

wort, JAR, 7.

CAG Grade & excert for

far end of lake, which is ey

Gmde 3-4,

CROSS SECTIONS

Pig. 6. Weebubbie Cave N2.

cause of the whiteness of their chalk, Here and there the roots rise in well-

rouuded domepits, beneath which the fairly level Hoors are broken by debris

piles. The largest example is found in Koonalda, where a dome rises about 225

feet between Second and Third Lakes and the zockfall piles NS feet high

beneath its almost perfect cupola. Width usually increases to 150-200 feet

at these domepits.

The plans of the deep caves are also simple, consisting of long, straight

halls which are probably joint-controlled, linked by rounded bends. In trend

they are directed coastwards in a broad sense but the alignments vary between

NW-SE and NE-SW, Only Koonalda has branches,

The Hoors are mainly formed of angular blocks and chalk dust on the one

hand and brackish Jakes on the other. Some earth and clay is also encountered,

ew, in the main passage of Koonalda. The lakes may be shallow measured in

a few inches 6r a foot or two, e.g. First Lake, Koomalda, or else they arc deep,

clear lakes, such as Third Lake in Koonalda and the lakes in Weebubbie and

Cocklebiddy. Soundings in January 1960 by J, B. Winwood and his party showed

GEOMOBPHOLOGICAL PROBLEMS, NULLARBOR PLAIN A3

the first two to be between 20 and 40 feet deep for the nost purt, Water levels

can vary quite substantially over intervals of several years, ct. at Teast 16 feet

in the case of First and Second Lakes, Koonalda, but they can alsu stay un-

changed for a year or two. Thus between Jamary, L957, and January, 1960, the

level of Weebuhbie Lake was unchanged, ‘The bottoms of the Jukes consist in

pitts ot mud anil in parts of angular blocks.

Ward (1946) has contuured a regional watertable in the South Australian

part of the Plain on the evidence from bores and the lakes of the deep caves

appear to Tie in this watertahle. “Karst watertables” are not accepted by many

Kuropean authorities, who insist that liinestone drainage takes the form of

ind¢ pendent underground streams whicl) do not conform to 2 single watertable

(cf. Lehmann, 1932), Nevertheless, the idea of a continuous watertable is prob-

ably accoptable in this context ob a leyel plateau in horivontally-bedded, litho-

logically-uniforin limestone of high porosity.

Abrukurrie differs from the others in several respects. Waterworn boulders

comprise much af the material on the steep initial descent and the nearly level

Hoor below is almost entirely alluviated with gravel and silt, the fincr material

being finmd at the lower end. Intermittent watercourses traverse the fill, Hnully

nioining wong and slightly erodiug the sidewalls, befare entering small holes in

the alluvium, These differences can be linked to the fact that a blind valley

wath it stream bed Jeads into this particular deep cave. Also Abrakurrie lacks

permanent! water bodies though a few inches of water may stand for short periuds

on the floor at the northem end of the main hall.

Wurbla also differs from the others in laying no large lakes. Beyond the

main, more or less horizontal, level between 150 and 200 feet down. there is a

finther descent over stecp talus, becoming confined where two small but deep

pools are reached with their sitfaces at 307 feet below the Plain (January, L957),

The five caves are restricted to the coastal zone of mallee, myall and mulga

scrub, King explained this distribution structurally, namely, that there is a

greater thickness of limestone near the coast, There is, however, more than

enough to accommodate the deepest known caves as tar north as the ‘Trans«

continental Railway; moreover, the waterlable fies law cnougly for deep caves,

Pussibly the coastal loealisalion is more apparent than real; the @oustal belt is the

hest known and deep caves may be discovered well inland, If uot, climate mav

be the responsible factor; the deep caves lie in the better watered part and four

of them exumined in 1937 Jay on the margin of fuirly large shallow depressions

in the surface of the Plain. The deep caves may be due to greater concentrati¢ms

of strtace runoff in the climatically more favoured helt,

Phreatic formation is attributed to the deep caves by King but his diseus-

sium shggests a confusion of distinctly different views on cave origins, those of

Duyis (1930) and Bretz (1942) on the one hand and of Swinnerton (1932) on

the ether. Davis and Bretz apply the term “phreatic” to sohition by nearly state

water and reaching to considerable depths beneath a weatertable, By. cortvitst,

Swinnerton stresses the importance of solution by rapidly moving water close ta

the watertable and in the zone of oscillation of Jevel of the watertable. Flow

divergent these views are is shown hy the fuet that Warwick (1953), when pre-

senting a general survey of theories of cave formation under a threefold divisiun

of “vadose”, “phreatic” ancl ~cumpromise™ theories, thought it most appropriate

ter ilistuss Swinnerton's views under the heading of “yadose” theory.

There has been much disevssiem of terminology in these matters (Glomvie,

1957, 1958; Little, 1957; Trstunan, 1957) and it is at least clear that “phreutic’

a J. N. JENNINGS

should be restricted to still or slowly moving water below the watertable, whether

oF HOt some such term as “epi-phreatic” he introduced to apply to Swinnerton’s

watertable streams,

The five grounds given by King for considering the deep caves as phreuatic

will now be discussed,

(a) “The cavern floors show little or no gradient.”

Allowing for rock piles beneath collapse domes, this seems to be substan-

tially true For the deep caves. More than half of Weebubbie has a steep gradient,

however, and Warbla has a lone steep descent below its level section.

However, this attribute is not characteristic of phreatic origins in the Davisian

sense, Solution well below a watertable will not be controlled by it; a truly

plieatic system is likely to be irregular im profile. I fact, slight gradient is

tuken hy authoritics such as Birat (1954) to be typical of well-developed vadose

cave systems. This criterion does not help much to distinguish between mature

vadose caves and those due ta Switnertan’s watertable streams, but it does argue

against phreatic formation sensu striato.

(b) “The general direction of the caverns (north-south) cotresponds with the

direction of wutertable drainage.”

Abrakurrie, Weebubbie and Warbla do indicate dramage towards the coast

influenced by the major joint systems.

Koonalda presents some difficulty in that, although the main passuge is

aligned roughly N-S, the deepest part is at the bottom of Third Lake at the

northern end. This ou its own suggests drainage against the gradient of the

watertable, However, the peotile could be due to irregular cave breakdown,

Thus t# the high domepit, between Second and Third Lakes, which reaches

within 50 feet al the surfuee ulccady, were to cause surface collapse, the Hoor

profile would he drastiewdly modified very quickly. There is other evidence

that drainage may have been seawards when there was active fow in the cite,

The branching puttern of the system is directed seaward and the current marking

in the flat passage linking West Passage with North-west Passage indicates a

svuthward flow. Koonalda is therefore regarded as compatible with King’s

eeneralisation. The 1960 survey indicates that Third Lake is about 5 teet higher

than Second und First Lakes so what seepage there is today is in the seaward

direction.

Awain, however, the interpretation of this generalisation favours Swinnerton's

ideas woud classical vadose theory rather than true phreatie solution, With the

former theories underground drainage will tend to hé dominated by streams

directed towards the coast. A phreatie pattern will be controlled much more

by structural conditions und elongation down the surface of the watertable may

vat he very strougly evident,

One additional fact possibly points to Swinnerton’s watertuble streams rather

than to completely free-surface gravity streams of simple vadose theory. At the

top of the steep talus slope in North-west Passage, Koonalda, there are large,

rounded chalk boulders implying rapid and turbulent How, but they are 40 feet

higher than the current markings in the squeeze at the far end of this passage.

This seems to imply uphill How under hydrostatic pressure ("conduits 4 eau

forece” of the French, e.g, Chevalier, 1944),

(v) “The oceurrence of caleite crystuls and calcite encrustration om the walls and

ceilings, in contrast to the absence Of dripstones. . . .”

MS, NULLARBOR PLAIN

CEOMORPHOLOGICAL PROBLE

‘ puadag 5 aprig Pap

PFE] USA d! OF FAPBLD GMD

(yes! wip 'Ajrey

F POCMUTE FALE BIARALTES

yN ZAVO VATVNOOM

J aaybes is]

SNOILD3S

oes

roe

39V55Vd

BLO YIO1 IK

fiesyag — a"

NV 1d

fete

few

YAW

VODEDZ

Koonalda Cave N4.

Fig. 7.

56 J. N. JENNINGS

The ubsence of dripstones is uo ground for phreatic origin of a cave. Not all

inactive vadose caves have dripstone decoration and conversely many caves

interpreted ws phreatio haye much ornamentation (Bretz, 1949). The difference

between the two types of cave in this respect is that stalactites and stalagmites

can develop in some degree during the active development of a yadose cave. but

nol during that of a phreatic one. However, a great deal of dripstone forms

after caves of both types have ceased being excavated and conditions have

chanved.

The explanation of the absence of dripstones must be sought elsewhere. It

may rest in the high porosity and sparse jointing of the Wilson Bluff Lime-

stone: water may soak through the body of the rock and is insufficiently con-

cuntrated in joint planes to break out in drips, Moreover, as has already been

noted, dripstone teatures are by no means plentiful in the shallow caves alsa,

the tutal amount of water seeping dowowards is small at all levels.

Calcite with external crystalline form is generally regarded as forming under

sull water. but the oceurrence: of such erystals on helietites, which there is na

reason to Ubink have been submerged in the course of their deposition, makes

this association far from invariable. “Crystal caves” are, nevertheless, vstally

associated with Davisian plreatic excavation, However, in his examination at

Abrakurrie, Koonalda and Weebnbbie. the writer was only able to find evlcite

crystals close to present lake levels, ew. in West Passage, Koonalda, Oseilatinus

of lake level such as are known today from this eaye could explain them,

(d) “The caverns have rounded cross-section and, in general, there is ne line

of demarcation of root and wall, The smooth and undulating surfaces of

both roof and walls are diagnostic of solutiou effects.”

The four detailed deep cave surveys availuble today — ie, of all except

Cocklehiddy — show that Mat roofs in bedding planes are found more widely

than the curved type and with them the line of mecting of reef and arched

wall is usnally well defined. Moreover, the wall arches often show keels along

bedding planes.

As has been mentioned above, the floors and lake bottoms are often covered

with angular rockfall. Uf the walls and roofs are dug to solution, why lasn't

this talus been clissolved also? Instead it is simpler to explain the forms as

duce ta weathering and bretkdown under eravity as Kine himself stiegests at

{mother point in his paper. The successively curved and keeled walls, thas Aat

raols and the domes constitute the equilibritun forms of mechanical breakdown

in this structural context of weak, uniform lithology in massive beds ot horizontal

altitude. Freshly detached blocks indicate adjustment is continuing slowly, as

dies the powdery outer surfuee of the walls aod the presence of chalk dust

an Jedges and floors. A further evidence of the readiness of Wilson Bhiff

Liniestone to weather is found in the large tefoni seen just in front of the Luke in

Weebubbie Cave (Pl, 4) and, not so well developed, close to the junetion of the

North-west and the main passages of Koonalda.

Mowever, at a fey points on the walls some rather weak eurrent markings

of larwe dirnensions are discernible; these, Jiowever, support vadose or Swintier

tows theory rather thin phreatic conditions,

(@) “The ends of the caverns arc as sudden as their commencement as sinkholes

and are rounded ont perfectly in continuity with the roofs and walls. Such

a phenomenon is not in accordance with the habits of vadose streams,”

The actual form of the apses would seem best attributed to the lithology

an¢l structure of the rocks. Whether the apses definitely end the caves. needs

GEOMORPHOLOGICAL PROBLEMS, NULLANBOR PLAIN 57

discussion, Abrupt closure is certainly evident at both ends of the long lull

of Abrakurrie, Beyond the apse at Warbla, there is the steeply descending

Passage mentioned earlier; collapse may have blocked a continuation here.

There is a water-filled continuation at the narth end of Third Lake, Koonalda,

whieh has still to be explored to its limit. Nor has the possibility of under-

water pussages leading on from the end of Weebubbie Lake been eliminated

as vet. At Christmas, 1961, a West Australian party dived at the far end of

the Lake and thirty feet beyond the roof séemed lo he rising into a further

chamber. Insufficient cquipment prevented further exploration, Diving at

Cocklebiddy Lake, the same party extended the known part of this cave. It

is Nat Anpossible that at Abrakurrie alluviation has buried former cuntimuation.

Despite these qualifications the fuel remains that very rapid changes in the

ize of the underground cavities are present even if there are prolongations uf

these caves vet to he penetrated, Such changes fit mast readily into phreatic

solution although the previous discussion has not favoured such an origin. Tesort

fannot be had to variations in rack strength to explain the cupid changes sinee

the horizontal uniformity of the rock is marked.

Asa whole, the discussion favours most of all Swinnerton’s theary of water-

table streams and Glennie’s adaptation of this theory to lis more general theory

of cuve development (Glenuie, 1954) appears to overcome the remaining difli-

cully better than any other. Caves start hy the preparation through phreatie:

sulution of small, interconnecting cayilies but large eaves are not generally

produced in this way. The next development is the enlargement of rising

stream passages under hydrostatic pressure at the outlets from the karst. This

improved outHow has the effect of draining the small unustomosing solution

tubes in the upper part of the system: vadose stream action and cave breakdown

proceed to enlarge these upper parts THowever, according to Glennie, the

most substantial cave excavation now tukes place whore these upper yadose

passuges meet the water-filled and tight plirentic elements still separating them

from the “artesian” final passages. Rains will cause much water ta bavk up

here and water levels will eseillate greatly. This is the loeus of maximum solu-

tion and produces the “master caves” as they are termed in Britain, the “hig,

level railway tunnels’, a description very apt for the Nullarbor deep caves also,

Glennie approximates this phase to Swinnerton’s theory und his modification

of Tt provides a possible explanation of (he sudden tightening up of the deep

caves.

‘There are difficulties, however, Solution tubes in the Wilson Bluff Lime-

slone ae few, although there are some examples which have been known to

spout water, The major joint planes, which appear to be responsible for the

straightess of some of the halls of the deep caves, may have induced more

phreatie tubes, however, DPinchemel’s views on the hydrological system al the

Chalk of N. Franco and S. Britain are relevant here (Pinchomel, 1954), Me

believes that there is a kayst watertable in the chalk but that beneath it localised

vorrents also occur, following joint systems. Such could have produced the

phreatic beginnings of the deep eaves, Secondly, the distanee to present or

former ondets on the coast or the Hampton Range is great and no such outlets

have yer heen identified with certainty, Caves in the cliffs Have been mentioned

hut not deseribed. Outlets ave likely to be submarine. of course, and I]. ¥. T.

Brown (1885) fos deseribed what he regacded as submarine springs offshore

at the Head of the Bight, Wilson Bluff ancl Merdayerrah, All that can be

cluimed, nevertheless. is that Glennie's theury provides the rnost likely working

hypothesis for the formation of the deep caves.

38 ].N. JENNINGS

ARE THE CAVES DUE TO PLEISTOCENE PLUVIALS?

In King’s view little cave development is tuking place today aud theretare

the caves must he attributed largely to greater solution during a Pleistocene

pluviul period. >

As has been seen already, the morpholozy of the caves testifies to cave

breakdown being the chief pracess in operation today; such sttean courses as

aecue give evidence of intermittent Wransport and deposition aud litthe of deep-

ening and widening of floors or walls. Cave excavation is clearly on a stall

seule, 4

As further evidence of this, King cited low lime content of the cave waters.

ilis three analyses can be supplemented by tour more from samples culleeted

in J§97.

Weebubbie Lake a. . 105 mg./1.

Virst Lake, Koonalda 105. meg./l. | Caco

Drip, Murrawijinice N7 233 meg./L. [ St

lirip, The Catacombs N20 237 myg./l. J

These values fall well within the range associated with active cave formation in

many Jrish karst areas for cxample. However, in arid areas the concentration

of solutes by evaporation must be allowed for. Thus do Corbel’s high values

trom Suharan limestone arcas of over 500 mg./], find their explanation (Corbel,

1957). Corbel alsu stated that “free CO.” is absent from Saharan waters. he

1957 samples from the Nullarbyr showed substantial “free CO.” contents. Tlow-

ever. subsequent investizutiow casts doubt on the validity af this determimation

as a measure of the capacity of natural waters for further salutiamal work. If

the Nullarbor Jakes are saturated at about 100 mg./L, this would lend some

support to the morphological evidence but it remains to be substantiated that

this is the case.

King gives low rainfall as an argument for very limited cave exeavation

today. This is indisputable and other factors intensify this effeet, Rainfall

effectiveness is reduced by high temperatures experienced in much of the year

and low relative humidities at most times. Vegetation cover is sparse even in

the coastal serabland and this minimises the supply of carbon dioxide to rain-

Water as it pereolates through the soil, Limestone solntian depends on carbon

dioxide in solution in the water und the chief sunrce of it is biological, [rom

surface trash and soils, Moreover, with the high temperature of undergvound

water here, the saturation equilibrtum in water of carbon dioxide, and so of the

carhonate jon, is lower than in colder climutes. These reasons combine tu

render hot, dry lands most unfavourable to cave development. On the other

hand, it must be admitted that meagre plant cover permits quicker minoff to

cave entrances. In this connection a quotation from T, Brown (1919) is rele-

vant, “T have known «a hundred acres of water 2 fect deep disappear in 6 hours

wid uext day when listening down a blowhole I heard water rushing through

the country below like a river”. Nevertheless, the overall picture is one of

inactivity in the caves today.

There is some evidence from areas close to the Nullarbor of a wetter

perlod (or periods) probably in the Pleistocene. King (1956) has described

Pleistocene-Recent lacustrine deposits, rising 36 feet above the present bed of

Lake Eyre. It is possible that the shift within these deposits from fresher con-

ditions below to more saline conditions above is the result of marine incursion

rather than a reflection of desiccation (Ludbrook, 1956). Nevertheless, the basal

GEOMORPHOLOGCICAL PROBLEMS, NULLARBOR PLAIN Bo

deposits suppirl the idea of a biv@er. fresher “L, Die? associated with moire

pluvial climatic enndilions. Soils evidence (Jessup, 1960) also points ta alter-

nating welter and drier conditions, Closer still, at Pidinga om the casters

marvin of the Plain, a chain of saline lakes linked by depressions blocked hy

wind-blown sands is regarded by King (1951) as relict froni an ancient river

systent and nutth-west of the Pie in Western Australia are chains of salt

lakes similarly thought formerly to be rivers draining down to it, From the

Plain itself there is little eviderice, however. Lamdelius (1957) has recently

described finds from eave fluor surfaces in the Nullarbor, which extend greatly

the range of certain small marsupials restrieted now within Western Australia

to the welter south-west, Thongh climatic change conld be the cause, Lun-

delins recognised that other explanations were possible also. More certoin

perhaps ts the older evidence (Cliuert, 1912) from Balladonia Soak on the

western margin of the Plain where fossil giant marsupials such as Diprotodon

sp. and Stheneus sp. were found in superlicial deposits of Pleistocere-Recent

wee. It is difficult to believe that these large animals could live off the vary

limited food stipply growing there nowadays, Even this is not conclusive.

however. Despite this lack of definite internal evidence. the presumption of

aawelter phase or phases is a reasonable one and much of the eave development

can he associated with them.

However, the vor of intense pertoration close to the surtace of the Pain,

if eurrectly interpreted as phreatic, implies a rise in the watertable as much

asx 200-300 teet uear the coast. Ih causing such a lowering, climatic change

evuld have been supplemented by coustal recession im some degree, but not

substantially, because the coastal evidence already cited snggests that recessiim

has not been very rapid, This big drup in water level seems ton much to be

attributed ta these factors,

King rejected changes in the relative level of land and sex as a contributery

cause in the development of the caves, Lut interglacial Ligh sea levels as pel

at the custatic oselllations of the Pleistocene (Flint, 1957) can he scarcely

denied though the very great eustutie oscillations chimed by some workers

may be. Moreover, there is the direet evidence from the Nullarbor coast af

higher stands in the relative level of land auc sea up to +120 feet. These

would seem to be a more adequate ¢ause of raised watertables. in the Plath

than climatic chanves of the arder usually envisaged for the Pleistovene:

Phrealic preparation can therefore be associated with the interglacial high sex

levels, ‘Vhe intervening pliases of lowered sea level during glacial periods would

then he pevinds of lowered watertables: lhoaweyer, with higher rainfalls, vadese

stream passages could be fashioned and master cave enlargement in accordance

with Glennie’s theory eould take place then

On this busis the shallow eaves would involve one high stand of sea level

wu of wittertable. Another may be the vause of fhe more or less herivontal

levels of the deep caves which stand high 2hove the present watertable, ie. thal

ot Warbla Cave and the North-west passage of Koonalda; possibly alsu this

applies to Abrakurrie, which seems to lie well above the present watertyble

(Jennings, 1961). The other horizontal levels of the deep caves, which eiptain

the lakes, may weed little oc mo change in seatevel to explain them und it is

possible that climatic change alone explains their present imactivity.

No correlations with the coastal evidence of sea-level changes are possible

as vel. but ft is evident that these changes are of the same order of importance

in tnderstundiug the development of the Nullarbor caves as is the changing

climate of the Pleistocene,

GQ) J. N. JENNINGS

IS THE NULLARBOR RICH IN CAVES?

Many writers haye maintained that the Nullarbor is rieh in caves, With

the Plain as little explored speleologically as it is, it is not easy to make a

reliable assessment of this. Obviotsly a distinction must he made helween

absolute wambers and the frequency of caves im relation to area. The numbers

of all cayes known at present probably does not umount to one hundred, cer-

tainly not ta two hundred, und this total comes from a limestone area of some

65,000 square miles, ie. roughly two and a half times the area of Switzerland.

Only a small proportion of Switzerland is of limestone, yet it has many more

vaves than that, including very mmch larger ones than any in the Nullarbor,

such as the Holloch, There are only five substantial caves known from the Nul-

lurhor at present; the small area of about three square miles of limestone at

Yarrongobilly, New South Wales, can match this, It is true that further

exploration in the Nullarbor will reveal many more caves. Yet certain parts

sheh as that arouud Nullarbor homestead are by now fairly well known and it

must be admitted that the caves are few and far between.

There is a strong likelihood then that the underground karst of the Nul-

larbor is as weekly developed as its surface developmeut discussed above.

One further aspect not previcusly mentioned is also congruent. Though the

Plain is a covered karst, ie. it ig mainly soil-sovered, there are rock onterops,

particularly around the collapse dolines and eave entrances. These outerops

are poor in minor surface solution features. There is little widening of joints

into solution slots or prikes; vertical or steeply sloping fuces fail to carry the

characteristic solution Huting (Rillenkarren) or solution wrooves ( Binnenkarren ),

The forms which occur are ny pittings and solution pans (Kamenitsa) of small

to moderate size on flat slabs or veutly inclined blocks: The fuct that the flat

bottoms of the pans are horizontal on onstubly inclined blocks indicate that

this surface solution is proceeding at the present time. The uct effect, how-

ever, has heen meagre. This contrasts drastically with the highly developed

surtuce solution featnres of the Limestone Ranges of the Fitzroy Basin (enaings

and Sweeting, in press); the latter receive rather more rainfull, 1825 inches,

but evaporation loss ts much greater,

The surface and the underground imorphology converge ta support the

couchision that here is a doling karst in au early stage of development despite

the long period of subaerial exposure sugwested by the absence of marine rocks

later than the Lower Miocenc, This is in agreement with the ideas of Birnt

(1954) and Corbel (1956) on the slow development of karst in semi-wrid and

arid climates, particularly in subtropical and tropical Tatitides. Though Pleis-

tocene phwial conditions appear to have ameliorated conditions and promoted

cave development, climate does not seem to have been Very much wetter for

very long periods, Vhe Nullarbor remains an immature, retarded karst.

ACKNOWLEDGMENTS

1 am indebted ta Dr. N. HW. Ludbreok for a vuluable disenssion of the

strettyraphy of the ares betore visiting it, As mentioned in the intvodnetion,

the work of the surveyors of the 1957 and the 1960 expetlitions has provided

much of the factual basis for this paper. They are toa numerous to acknow-

ledue individually, but for the surveys on which the accompanying figures ave

baved, Mr, R. T. Sexton and Mr. J, B. Winwood must be specially thanked.

Mr H. Berry, Australian National University, analysed the water samples re-

GEROMORPHOLOGICAL PROBLEMS, NULLARBOR PLAIN 61

corded here and he has many times advised me on chemical matters. 1 must

also thank Myr. H, Fairlie-Cuninghame for allowing his photographs to he used

for Plates 2 and 3,

REFERENCES

For a mote comprehensive list, see Jenninus (1961),

Binor, P., 1954, Problémes de inorphologie karstique, Ann, Géogr., 63, pp. 161-192.

Boe, tA 1942, Vadose and Phreatic Features of Limestone Caverns. J. Geol, 50, ppr

Oe «

Buerz, J. H., 1949. Gailsbad Caverns and other Caves of the Guadeloupe Block, New

Mexico. J. Geol., 57, pp. 447-463,

Brown, H. Y. L., 1885, A Report on the Geological Character of the Country Passed

over from Port Augusta lo Eucla, S. Aust, Parl, Papers No, 45.

Brown, T., 1919. Nullarhor Plain. Proc. $. Aust. Br. geogr, Soc. Anst., 19, pp, 141-152.

Crrvarier, P., 1944, Distinction morphologique entre deus types d’érosion souterraine.

Rev. Geogr, Alp., 32, pp. 475-192,

Coneman, A. and Baucuin, W. G. V., 1959. The Origin and Development of Surface De-

pressions in the Mentlip Hills. Proc, Geol. Ass. Lond, 70, pp. 291-309.

Cian, I 19357, Les Kursts de neard-ouest de l'Europe. ,,- Mem. Inst. Etudes Rhodaniennes

o. 12.

Coron, C. A. 1951, Atlantic Gulfs, Estuaries and Cliffs, Geol, Mag., 88, pp. 1154124.

Davin, E. E., ed. Browne, W. R., 1950, The Cealogy of the Commonwealth of Australia,

Arnold, London,

Davis, W. M.. 1930, Origin of Limestone Caverns, Bull, geod, Sac, Amer,, 41, pp, 475-626.

Frost, M, J., 1958, Jointing Assaulated with the Hampton Fault near Madura, W.A. J. roy,

Soe. W. Aust, 41, pp. 25-26.

Ginsow, ©. G., 1900. Geological Features of the Couritry Lying along the Line of the

Proposed Route of the Transcontinental Builway. Bull, geol. Surv. W. Aust, No. 37.

Graven, L,, 1912. Fossil Marsupial Remains frorn Balladonia in thy Kucla Division, Ree.

West. Aust. Mus., 1 (2), pp. 47-63.

Cratssscn, M. F., and Pantin, 1. W., eds, 1958 The Geology of South Australig, J, geok

Soc, Aust, 5 (2), pp. 1-163,

Guus, I. 1954. The Origin and Developmeyit of Cave Systems in Limestone, “Trans.

Cave Res. Group, Great Britain, 3, pp. 75-63.

Ceunsiz, E,, 1957. Phreatie anc Artesian Water. Cave: Res. Group, Great Britain News-

letter, 63-4, pp. 14-16.

Guennie, E., 1958. Nameless Streams: Proposed New Terms. Cuve Res. Group, Great

Britain Newsletter, 79-80, pp. 15-14.

Junsuncs, [| N,, 1961. A Preliminary Report on the Karst Morphology of the Nullarbor

aims. Cave lixp). Group, §, Aust, Occ, Pap. No, 2.

Jvssor, Bo W.. 1960. Identification anc Signilicance of Buried Soils of Quaternary Age in

the South-Eastern Portion of the Australian Avid Zone. J. Soil Ser, 11, pp. 197-205.

JONES, ]. Vis 1880, Examination of the Country North-East of Encla, S$. Aust, Parl. Papers,

wo, TO),

Kine, D:, 1950, Cevlogiex! Notes on the Nulkivhor Cavernous Limestone, Trans. roy. Soe.

S. Aust, 73, pp. 52-58.

Kine, D,, 1951. Geology of the Pidinga Area. Trans. roy. Soe, S, Aust,, 74, pp, 25-42,

Kine. D., 1956. The Quaternary Strativvaphic Reeard al Lake Ryre North and the Evolution

of Existing Topographic Morms. Trans. roy. Soe. $. Aust. 79, pa. 95-103,

Lidirann, O,, 1932, Die Hydrographie des Karstes, Deuticke, Leipzig.

vai Wt 1957, A Nameless Stream, Cyve Hes, Group, Great Britain, Newsletter,

15, p.

Lununoon, N, HL, 1956. Microfussils from Pleistnesne ty Recent Deposits, Lake Eyre, South

Australia. Trans. roy. Soo. $, Aust, 79, pp. 37-45,

Lunuuoox, N. H., 1958, The Stratigraphic Sequence in the Western Portion of the Encla

Basin. J, voy. Sou, W. Aust., 41, pp. 108-114.

62 J. N. JENNINGS

Lupsroox, N. H., 1961. Subsurface Stratigraphy of the Maralinga Area, South Australia.

‘Trans. roy. Soc. S, Aust., 84, pp. 51-60.

Lunpetius, E., 1957. Additions ta Knowledge of the Ranges of Western Australian Mammals.

West. Aust, Nat., 5, pp. 173-182.

Pincurme., P., 1954. Les plaines de eraie. Colin, Paris.

Strpuens, C. G., 1961, ‘the Soil Landscapes of Australia. Commonw, Sci. Ind. Res. Org.,

Soil Pub, No. 18.

AWTS, A. C., 1932. Origin of Limestone Caverns. Bull. geol. Soc. Amer., 43, pp.

663-694.

Tare, R,, 1879. The Natural History of the Country around the Head of the Great Australian

Bight. Trans, roy. Soc. S. Aust., 2, pp. 94-128,

THomson, J. M., 1950. The Nullarbor Caves System. Trans. roy. Soc. 8, Aust., 73, pp. 48-51.

THATMAN, E, K., 1957. A Nameless Stream. Cave Res. Group, Great Britain, Newsletter

68-69, p. 6.

Vauentin, H., 1952. Die Kiisten der Erde. Petermanns geogr, Mitt, Erg. No. 246.

Warp, L. K., 1946. The Gecurrence, Composition, Testing and Utilisation of Underground

pha South Australia aud the Search for Further Supplies. Bull. geol. Surv. S. Aust.

o, 23,

Warwick, G. T., 1953. The Origin of Limestone Caves, Ch. IL of British Caving, ed.

C,H. D. Cullingford. Routledge and Kegan Paul, London.

Woopwanp, H, P., 1890. Ann. Gen. Report Govt. Geol. W. Aust. for 1888-9. Govt.

Printer, Perth,

Woo tnoucn, W. G,, 1933. Report on Aerial Survey Operations in Australia during 1932.

Govt, Printer, Canberra.

J, N. JENNINGS Puate |

sgt 2 = =

Fig, 1. Black caleite infilling anastomosing solution tubes in the Nullarbor Limestone in

White Wells Cave N14. The left of the photograph comprises about 3 feet vertically of

rock face.

Fig, 2. Tafoni on the wall above the lake of Weebubbie Cave. About 70 feet vertically of

rock face is visible and the tafoni go up to 3 feet across in size.

“Trans. Roy. Soe. S.A.", Vol. 87.

}. N. Jennincs PLATE 2

Vig. 1. View along the North-West Passage of Koonalda Caye N4, Behind the figures there

is the steep rise of 70 feet to the upper level of this passage, The angular rockfall and

chalk dust covering the floor are typical of the deep caves of the Nullarbor.

Photo by H. Fairlie Coninghame.

The lake in Weebubbie Caye N22. [t is 20 to 40 feet deep and crystal clear, Flat

roofs and arched walls are common in the deep caves.

Photo hy H. Fairlie Coninghame.-

“Trans. Roy. Soc. $.A.", Vol, 87.

FLORA CONSERVATION IN SOUTH AUSTRALIA

PT. 11. THE PRESERVATION OF SPECIES RECORDED IN

SOUTH AUSTRALIA

BY R. L. SPECHT

Summary

A list of plant species recorded in the flora and fauna reserves in South Australia is given. This

information is examined against the total flora of the State. 42 p.c. of the 2,255 native species and

4,3 p.c. of the 557 introduced species are found on the present reserves, The distribution of the

species, not conserved, is examined to pinpoint the sites of future reserves,, Sites in the Musgrave,

Everard, Mann, Birksgate, Gawler or Northern Flinders Ranges would enable almost 50 p.c. of the

remaining flora to be conserved. Small areas on the adjacent, more uniform plains would enable

appropriate plant formations to be preserved. Sites along the River Murray would conserve up to

8 p.c. of the remaining flora. While sites in the Southern Flinders Ranges, Burrs Hills, foot of Yorke

Peninsula, Fleurieu Peninsula and north of Mt. Gambier are suggested to conserve a considerable

number of the other species as well as plant formations. The problem of introduced species is again

discussed.

FLORA CONSERVATION IN SOUTH AUSTRALIA

PT. Ll. THE PRESERVATION OF SPECIES RECORDED IN

SOUTIL AUSTRALIA

by R. L. Seucur*

(with Collaboration from J, B. Currant) t

[Read 13th September 1962

SUMMARY

A list of plant species recorded in the flora and fauna reserves in South

Australia is given. This informati¢en is examined against ihe total Hora of the

Stite. 42 p.c. of the 2,255 native species and 43 poo. of the S57 introduced

species are found on the present reserves

The distribution of the species, mot conserved, is examincetl to pinpoint

the sites of fitere reserves.

Sites in the Musgrave, Everard, Munn, Birkygate, Gawler or Northern

Flinders Ranges wonild enable almost 50 p.c, of the remaining flora to be con-

served, Small arcas on the adjacent, more uniform plains would enable

appropriate plant formations to be preserved,

Sites along the River Mnrray would conserve up ta 8 pic, of the remaining

flora. While sites an the Southern Flinders Ranges, Burra Hills, foot of Yorke

Peninsula, Flenvica Peninsula ancl north of Mt, Gambier are suggested to

cunserve a oonsiderible nnimber of the otler species us well as plant formatians,

The problem of introduced species is again discussed,

INTRODUCTION

In the previous volume of these Transactions the authors (1961) discussed

the preservation of the various plant formations and assuciations which had been

recorded in Sonth Anstralia. Glaring deficiencies were indicated,

In this paper din attempt has been made to tabulate the plant specics ( Ferns,

GCymnosperms, and Angiosperms only) which muy be found in the Reserves

eslablished in South Australia up to this date (Table L). For some of the Re-

serves the list is by no means complete, but it serves to highlight major dis-

crepancies in flora conservation in this State.

The records thus tabulated were compared with the list of species recorded

for South Australia by Black (1943-57) and subsequent workers (\Villiams,

1953; Tsing, 1955, 1958 and 1961; Acllen, 1953; Garden, 1956; Melville, 1957 and

1960: Wichler, 1958; Forde and Ising, 1958; Stauffer, 1959, Wilson, 1060. and

1961; Symon, 1961; Burbidge, 1953, 1958 and 1960; Willis, 1957 and 1958;

Carolin, 1958 and 1961).

In each family the number of native und introduced species recorded in the

Reserves was compared with the total listed for the State. The distribution of

any species not, as yet, recorded in any reserve was then examined on a regional

basis; these data, compiled for cach family and for Use whole flora of the State,

ure presented in Table 2.

Austria,

Trans, Roy, Soc, S$, Aust. (1963), Vol. 87.

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FLORA CONSERVATION IN S.A.— PART II 85

TALLE 1—LISY OF STECIES RECORDED IN FLORA AND.

FAUNA RESERVES 1N SQUTH AUSTRALIA—continued

Species i? 3 4 45 6 7 $ H WIL 1218 j4

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DISCUSSION

The data presented in both Tables 1 and 2 indivate that, of the total at

2,255 native species listed for South Australia, only 942, i.e, 42 p.c., have been

recorded in Reserves. The remaining 1,313 species not conserved are scattered

widely throughout South Australia. The data presented at the end of Table 2

indicate the number of these latter specics that have been recorded for any

particular region within the State. As many of the species concerned are wide-

spread, they may be included in several of the regions; conversely, a number

may he quite localised.

The Region embracing the North-East and Far North contains by far the

grcatest number (610) of species, in fact, 46 pic. of the flora not conserved.

It may be argued that the flora of this area is in no danger of extinction, The

Simpson Desert is included within this area; its small flora (76 species according

to Fardley, 1946) is certainly in no danger of extinction. The rest of the region,

however, is largely under pastoral lease for cattle and sheep grazing. As may

be expected in arid regions, rates of stocking are low, but unfurtimately, even a

small error in stocking rate may lead to overgrazing in times of drought. In the

pust severe overgrazing has occurred in this area and has led to the large-scale

destruction of vegetation with subsequent erosion, All areas are grazed by

rabbits which often reach plague numbers. No area can he said ta he ungrazed

hy introduced animals, Scedlings of shrubs and trees have been destroyed

(Wood, 1936) until, new, regeneration of much of the vegetation may be im-

possible unless properly protected from grazing animals,

Many of the species recorded for the previous region extend westward

into the Flinders Ranges, North-West, Nullarbor Plain, the Gawler Ranges of

Northern Eyre Peninsula, and also southward into the northern part of the

heterogencous Murray Lands. lu fact, many of the species extend into the

drier habitats of the southern, higher rainfall districts. In all, about 900 species

(69 p.c.) of the 1,313 species at present mot recorded in Flora and Fauna

Reserves nay be found in some part of this arid region.

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f puvps] comeSury (A)

L yNsutteg eyo (41)

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‘¥VITFULSNY HIDQOS NT SAANHESHH NI

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VIIVILLSIY HLOOS NI SUAYWESHY AI GACH OORN SHIOMdS CADACOMLAI ANY GALLYN 40 YHEWON HHL TO NOsTH¥d tO)

‘*@ ATA,

8&6

FLORA CONSERVATION IN S.A,— PART IL

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YO) R. L. SPECHT

This large suite of specics. contains imany families characteristic af atid

regiims, few of which are conserved, e.g.. Koonamore Vegetation Reserve is the

only Arid Zone Reserve in South Australia and this is a mere 960 acres in areca

(Specht and Cleland, 1961). Many of the species, althauxh widespread in the

arid zone are confined to particular mierchabitats. Some areas such as the

Nullarbor Plain, Great Victoria Desert, Sturt’s Stony Desert and the Simpson

Desert are comparatively uniform. In the mimges, however, and on the sur-

riding plains a geeut diversity of microhabitats is found; there the greatest

range of species occurs. The Musygtave, Everard, Mann and Birksgate Ranges

of the Far North-West, the Gawler Ranges of northern Eyre Peninsula, the

northern end of the Flinders Ranges, are all situations where a wide range of

species characteristic of the arid zone anay be found. Reserves in any of these

areus would not only conserve: a large percentage of the State’s flora, but would

he scenically attractive to tourists.

However, such areas with their wealth of microhabitats usually do not allow

the satisfactory development of extensive plant formations. The low lavered

woodland, shrub steppe and semi-arid tussock vrassland formations (see Specht

and Cleland, 1961) and their characteristic plant associations often interwrade

ta such-an extent in such reas as to be defined with difficulty, The preservation

ol such formations is best made in more uniterm habitats. Appropriate steps

should also be taken to have selected arcas un uniform sites (say, 10 square

miles in area) of cach formation (and association, if possible) proclaimed as

Reserves, and adequately pratected from rabbits and other introduced animals.

These areas will it be attractive to the tourist but will he of inestimable

interest to future scientists. LF possible these could be chosen adjacent to the

mon scenic range country.

Of the 100 other species not conserved in South Australia, about 100% may

he toand confined to the corridor of the River Murray, Suitable sites. burderine

on the Murray should be sought tu conserve some ol these species; these sites

should also be suitable us sanctuaries for birds which abound along the Murray,

The other 300 species are scattered irregularly throughout the sonthern

part of the State. A number huve been found in very limited ateus, and, in

some cases, are already extinet, others may be only westerly extensions of species

frum the Eastern Stites into the South-Rast of South Australia.

Tt is difficult ta pinpaimt possible areas for future reserves to conserve the

other species, The. figures given in Tuble 2 underestimate the possible number

ot species (not conserved) to be fonnd on Yorke Peniwsula and Kangaroo

Island, becanse Black (1943-57) usually humps records from these regians with

the Mt. Lofty Ranges-Mid North xegion in his “Southern Wistricts”.

Areas such as the southern Flinders Ranges, the hills near Burra, the foot of

Yorke Peninsula, the southern part of the Flenrien Peninsula and the dune-

‘atye and swamp country north of Mt. Gambier should preve worthy of ives

tigation foe future reserves, These should be examined nat anly in the Hight of

the plant species they may canserve but also in the light of the plant tovmatinns

aud associations found in the area (Specht and Cleland, 1961).

tt is pointless to insist that any of the 557 introduced plant species should

be conserved, although in afew cases potential economic plants muy be invulvedt.

It ts interesting, but probably cofucidence, that 43 p.c, uf these introduced

species are now found on the present Flora und Fanna Reserves ~ ils the same

percentage as that of these native species (Tuble 2). This invasion of reserves

LORNA CONSERVATION IN 5.A.—PART U 1

by introduced species emphasises the problems of maintaining Hora aod fauna

reserves discussed in the first paper in this series (Specht and Cleland, 1961).

Steps should he taken to avoid this contamination. Ltmay be impossible in such

plant formations as the savannah woodland and mallee, but not so difficult in

the other formations if contamination by rubbish and fertilizer dust is avoided,

ACKNOWLEDGMENTS

This study provides further background information for several bodies in-

terested in Nora conservation in this State. Much of the field data was gathered

by the authors while members of the Flora and Fauna Investigation Committee,

1960-41. The co-operation af other members, Mr. O. Bowden (Chairman) of the

South Australian Lands Department, and Mr, A.C. Boge of the South Australian

Depariment of Fisheries and Game, was greatly appreciated.

Further data were provided by Mr. D. I=. Symon of the Waite Agricultural

Research Institute (Wilpena Pound) and Miss C. M. Eardley, of the Bolany

Department, University of Adelaide (Koonarmore Vegelation Reserve),

Dr, Hj. Kichler and Mr. P, G, Wilson of the State Herbarium of South

Anstralia, Mr. GC. D, Boomsma of the South Australian Woods and Forests De-

partment (Eucalyptus), Dr, RoC. Carolin of the Botany Department, University

of Sydney (Geraniaceae), and Dr, §, T. Blake, Herbarium, Brisbane ( Aizoaceae)

checked ‘the identification of the plants collected. Their assistance is gratefully

acknowledged,

REFERENCES

Avi orn, PL, 1955. A New Species ot Atriplex (Atiplex sponpiinaleiy Acllen). Titus, Roy.

Soe. 8. Aust. 78, p. 155,

Buaek, J, M., 1943-57, Flora of South Australia. Vols. 1-4, 2nd od. Covt. Printer, Adeluide.

Braxe, §. T., 1959, New and Noteworthy Mants Chiefly from Queensland, 1) Proe, Roy.

soc, Qld, 70, pp, 33-46,

Rurnwer. Nancy U., 1953, The Genus Trivdia RB. Bro (Graminewe). Aust. J. Dot, 1,

pp. 121-184.

Bunginer, Nanev ‘I, 1958 A Monographic Study of Hetielrysaum, Subgenus Oaothamnus

(Composite) and of wo Related Genera Formerly iuchuled therein, Aust. J. Bot, 8,

pp, 229-284,

Bunsen, Nancy 'T., 1960, The Australian Species of Nicotiuna TL, (Solanaecac). Aust. J.

Bat, &, pp. 342-380,

Canouis, BR. C., 1958. The Species of the Genus Brodivw L'Aer, Eudeinie to Australia.

Proc. Linn. Soe. N.S. Wales, 83, pp. 92-140,

Canuun, KOC, 1961. The Genas Pelargonium L'Aeér, es Ait, in Australiq, Proe. Tron,

Soe. NUS. Wutes, 86, pp. 280-254,

Cinuanp, J. B. 1995, The Plants of Chaunegy’s Line, 8. Aust. Nat,, 80, pp. 9-13.

Corusan, ). B. and Buaex, J, M., 1927, An Enumeration of the Vaseular Plants of Kangaroo

Istund, "rans. Roy, Soc, S. Aust. 51, pp. 24-67.

Onunanp, J. B., aod Biack, JoM., 1941. Au Entirnesration of the Vasenlar Plints of Kounipearco

Island, Additions ane Corrections, “Trans, Rey. See. So Aust, 65, pp. 244-248,

Ciratn, J. B. and Brace, J. M., 1952. An Evumeration of the Vaxeular Plants of Kangeuran

Island, Seennd List of Adeitisns and Correetions. rans. Roy. See. $. Anst., 75,

pp. 22-24,

Ciunano, |. B,, and Gonnsack, H., 1953. Plants of the Mount Lofty Ranges. Pp. 161-107

in “Nutional Pack and Reserves”. Govt, Printer, Adetaicde,

Coanpnane, J. B., 195), The Clinute, Geology. Seils and Plant Kenlogy of Partion ef The

County of Boekinghan (Ninety Mile Plain), South Australia. C.S.1.R.O, (Aust) Bull

No, 266.

Courr, A.B. WaT. Chlimens in the Nomenclature of some Victoriim Dieotyledons. Vixt

Naf, 73, pp. 173-6.

98 R, L. SPECHT

Fanotey, C. M., 1946, ‘The Simpson Desett Expedition, 1939, Scientific Reports No. 7,

Botany—Part (; Catalogue of Planty. Trans. Roy, Soc. §. Aust, 70, pp, 145-174.

Eicuies, Hj, 1956. The Ranunculus. sessiliflorus Group in South Australia. Trans, Roy.

Soc. 5, Aust., 81, pp. 175-J83,

Forpe, N., and Isesc, E, H., 1958. Acacia caleivola, a New Species of Importance to the

Ecology af the Australian Arid Zone, Trans, Roy. Soe. $. Aust., 81, pp, 153-160.

Ganpen, Joy, 1956. A Revision of the Genus Callitris Vent. Contrib. N.S. Wales Nat. Hers,

2, pp. 363-92.

lsinc, WL IT, 1955. Notes on the Flora of South Australia, No. 6. ‘Trans. Roy. Soe, S. Aust.

78, pp. 110-120,

Isinc, EB. H., 1958. Nutes on the Flora of South Australia. No. 7, Trans. Roy. Soc. $-

Aust, 81, pp. 165-173,

Isinc, EK. H., 1961. Bassia uniflora (P.y.M,) R.Br. (Chenopodiaceae) and Allies mm Aus

tralia. Trans, Roy. Suc. 5. Aust. 84, pp. 87-98,

Jonson, L, A. S, 1950. A Llitherto Undeuseribed Koehia (Chenopodiaceae), Contrib.

N.S. Wales Nat. Herb., 1(6), pp. 343-345,

La Bruarmerr, J. J. H. oe, 1799, Belation du Voyage 4 la Recherche de la Pérouse. Vol, 1.

(Jansen: Paris, }

Lircurieio, W. H., 1956. Species Distribution aver Part of the Coonalpyn Downs, South

Australia. Amst, J, Hot., 4, pp. 68-115,

Minvitne, B., L57. A New Frunkenia from Suuth Australia, Trans. Roy. Soc. $, Anst., 80.

pp. 144-145,

Metvitte, H., 1960. An Aberrant Speeies of Eelipia frou Australia, ‘Trans. Roy. Spe, $.

Aust., 83, pp. 77-78.

Ossorn, TG. B., 1923. The Flora and Fianna of Nuyts Archipelago and the Investigator

Group. No. 8 Che Evology of Pearson Island. "Lrans. Roy, Soc, S, Aust, 47,

pp. 97-118,

Svecuy, R. 1... 1963, Durk Island Heath (Ninety-Mile Plain, South Anstrilia), VII. The

Effect of Fertilizers on Composition and Growth, 1950-60. Aust. J. Bot., IL, pp, 67-94,

Sreour, KR. L,. and Curranp, J. B., 1961, Flora Conservation in South Australia, 1. The

Preservation: of Plant Forinations und Associatiauy Recorded in South Australia, Trans,

Roy, Soc. S. Aust., 85, pp: 177-196,

Spout, R. L., und Rayson, Paraicra, 1957. Dark Island Meath (Ninety-Mile Plain. South

Australian), L Definition of the Ecosystem, Aust. J. Bat,, 3, pp, 52-85.

Sraveren, H, U,, 1959. Revisin Anthobolearum. Mitt. Bot, Mies. Unive Zurich, Na. 213;

jyMon, D. E., 1961, Whe Species of Oralis Established in South Australia. ‘Crans: Tay.

Soe. S. Ast, S34. pp. 71-77,

Wintisss, L. D., 1953. Notes on South: Australian Grasses. Trans. Roy. Soo, $, Anst., 76,

pp. 5-55,

Wiiaas, J. A. 1957. Vascular Plora of Victoria and South Australia, Vict. Nat,, 73, pp:

168-202,

Wricis, |. WL, 1958. Vaseular Flora of Victoria and South Australia. Vict, Nat, TA, pp. 84-6,

Wieson, PL G.. 1960. A Consideration of the Species Previonsly ineluded within Helipternni

albicans (A. Cann.) DC. ‘Vrans, Ray. Sec. §. Aust, $3, pp. 163-177.

Winson, 2. G., 196]. A Taxonomic Revision of the Genus Correa. “Trans. Roy, Sou, §,

Aust, 65, pp, 21-53,

Woop, J. C., 1936, Regeneration of the Vegetation on the Koonaraure ¥ eeetation Keserve.

1926 te 1986. Trang. Roy. Soe, S. Anst., 60, pm. P6-I1L.

ERRATA

In Flora Consercation in South Australia. Part I, by Specht aud Cleland, Trans, Roy. Soe,

South Australia, 85, pp. [77-196 (3961).

P. 180. Under “Tussook Grassland Association (i1)”, read “Lemandra thura-Lomanidra eff test

(irongrass) association” tustead of “L, dura-L. multiflare . . . association, The

geous Lomendra is dificult taxonomically.

PL 192. Nest-te-last paragraph, Myoperum ylutyearpuin is not resirteted to the east of

the Flinders Range as stated, but is alsa quite veminon west of this Range from

Pert Cermem northwards.

THE PLANT ECOLOGY OF LOWER EYRE PENILNSULA,

SOUTH AUSTRALIA

BY D. F. SMITH

Summary

A detailed study has been made of the plant ecology of Lower Eyre Peninsula. Archaean rocks,

lateritic peneplain remnants and calcareous loess have, in various combinations, formed a wide

variety of soils; and with a mean rainfall range from 12-23 inches per annum, a wide variety of

plant habitats is provided. The autecology of 21 Eucalypts and three other species is discussed,

some in detail. Special interest centres on Eucalyptus cladocalyx which here has its largest area of

natural occurrence. The plant communities are grouped as malice, woodland or sclerophyll scrub

and the floristic composition of each is given. A vegetation map has been compiled. As virtually all

the of the species present are distant from their main location, their presence and extent of

occurrence have considerable ecological significance. This is discussed in relation to recent climatic

history and evidence is presented for retreat and survival as relic patches, rather than long distance

dispersal and colonisation.

THE PLANT ECOLOGY OF LOWER EYRE PENINSULA,

SOUTIT AUSTRALIA

by D. F, Syerma*

(Communicated by D. LE. Syino)

[Read 13 September 1962]

SUMMARY

A detailed study has been made of the plant ecology of Lower Eyre Penin-

sula, Archaean rocks, lateritie peneplain renmants ond calcareous loess have, in

various combinations, formed a wide variety of soils: and with a mean rainfall

range from 12-23 inches per annum, a wide variety of plant habilats is provided.

The autecology of 31 Encalypts and three other species is discussed, some in

detail. Special interest centres on Lucalyptus eludiealiyx which here has its

largest area of natural oceurrence. The plant communities are grouped as

mallec, woodland ar sclerophyll scrub and the Horistie composition of cach is

viven. A vexetation map has heen compiled.

As virtually all the of the species present are distant {rom their maiu loca-

tion, their presence and extent of occurrence have considerable ecological signi-

ficance, This is discussed in relation to recent climatic history and evidence

is presented for retreat and survival as relic patches, rather than long distance

dispersal and colonisation.

INTRODUCTION

The large variety of soils and the wide range from 13-24 in, of average

annual rainfall in Southern Eyre Peninsula makes it an interesting area for

ecological study. The woodland areas were occupied as early as 1840, but

the mallee and sugar gum scrub have mostly been settled and cleared sinee

1900. This settlement has modified some plant communities and almost obliter-

ated others.

PITYSICAL, ENVIRONMENT

1, Gronocy

The geology uf the area has been described by Johns (1961). Ecologically

the lateritic areas and the Recent und Pleistocene sands and limestone are

important. Their distribution and relationship to other areas has been discussed

by Smith (1960).

2. PrrvstocrRaArry

Most of Lower Myre Peninsula is gently undulating with some resistant

cores of quartzite forming small ranges up to 1,400 ft. high on the western side.

On the custern side, the Koppio Hills extend from near Port Lincoln northward.

They are capped in imany plages by remnants of a lateritic plateau, sloping

gently from 8-900 feet in the north to 600 feet in the south and bounded hy

a definite fault line on the eastern side, The relationship of toposraphy ta

soil type, vegetation and Jand use is summarised in Fig, 2.

* Now of the School of Agriculture, University of Melbourne.

Trans. Roy, Sec. $, Aust. (1963), Vol. 87;

St D. F. SMITH

3. Dratxace

The Tod River is the largest watercourse in the area, and it is rarely peren-

nial. In the moister parts of the Koppio Hills, spring-fed streams do flow in

the summer, but ure soon lost in stream bed gravels, forming moister habitats,

Flooding by westward flowing streams has apparently influenced soils and

vegetation, especially near Cummins. These drainage lines have been dammed

back by the development of aeolianite dunes (or the accumulation of siliceous

sands } forming salt lakes and swamps with much water passing into the aeolianite

or sands, providing habitats for patches of Eucalyptus camaldulensis (red gum)

vegetation, The acolianite may act as an important aquifer, especially when

resting on impermeable Archacan rocks (Johns, 1961).

CLIMATE

A detailed study of climate is not possible due to the absence of recorded

data other than for rainfall which is reasonably covered. Crocker (19464) has

summarised the available data for the whole peninsula. The climate is typically

Mediterranean with 70 p.c. of the rainfall in the May-Oetaber period and a

long, hot, dry summer.

The sivnificance af the raimfall clatu for native species, many of which are

perennial and summer-growing, is quite different to that for agricultural crops

dependent on winter-spring conditions. Soil moisture storage front winter rains

will be very important and soil tvpe will modify rainfall effects on native yege-

tation more than for winter wuual growth,

Since recording began there appear to have been no periods likely to seri-

ously affect the native plauts, Le. no run of wet seasous or very dry ones, At

Cummins the year 1957 was very dry (S in.) but it followed the wettest year

un record (almost 25 ins.). Thus while 1957 was disastrous agriculturally it

had little effect on native vegetation because of suil stovage from the previous

Var,

A rainfall map (Fig. 1) has been compiled using data for the 1916-57

period, mostly supplied by the Commonwealth Bureau of Meteorology with

some interpolation from, farmers’ records, ‘Tho ayerage rainfall for the period

1941-57 Nas seldom ecyualled the 1911-40 (“normal” period) average, Most of

the Koppio Ilills and Cummins area has received below “uormal” by as much

as 3-2 inches at Green Patch — while north of this has been above “normal” —

1-1 inches at Yeelanna. Thos use of the 30-year normal has becn misleading

in carlier maps, especially in drawing the 16-inch isohyet near Yeelumna,

The annual average rainfall at Cummins from 1916-57 was 17-32 inches with

a TmHean variation Of 17 pic. Gr 3-0 inches,

In 46 p.c. of the years recorded rainfall was within 3-0 inches of the mean

and in only 7 p.c: has the variation heen #reater than 6 inches.

SOLLS

The only detailed soil survey carried out in the area is that of Stephens

(1943) who surveyed a small area of Jateritie seils near Wanilla prior to its

use for Soldier Settlement. Howeyer. knowledge of the area las been jourcased

by the work of Crocker (19468, bj, French (1955) and Sinith (1960). A

survey of a partion of Kangaruo Island by Northcote and Tucker (1945) is of

interest in the close similurities of sume soil types.

PLANT ECOLOGY OF LOWER EYRE PENINSULA, 5.A. 95

The ecologically important soil groups are—

1. The Lateritic Derivatives

These are the most widespread group. Normul lateritic soils with a sandy

A horizon are widespread in the Koppio Hills on wider divides, on the gently

undulating Wanilla area (Stephens, 1943) and on the western side of the

peninsula near Coulta and Kapinnie. Shallower lateritic grayelly sandy loams

and gravelly clay loams occur where truncation has occurred.

These soils are generally acid (except in the north where much lime. is

present), have poor water-holding capacily, low nitrogen and phosphate status

and lew total exchangeable cations.

LAKE HAMILTON KOOLIDIE

LAKE WANILLA

WANGARY

Fig. 1. Loeality and rainfall map.

9. Red-brown Earths

A. number of areas of typical red-brown earths haye developed, especially.

along the eastern side of the Koppio Ilills, On the western side near Cummins

and to the north near Unyarra, a wide range of red-hrown and brown-grey

suils af varying texture (but usually clay) have been formed on the outwash

materiil from the hills. Varying additions of calearcous loess, siliceous sand

and eyclic sult have contributed to the present complex mosaic of red-brown

earths, heavy grey clay loams, solonised brown soils and solodic soils. Physical

and chemical characteristics of these soils vary tremendously. They are usually

just alkaline, and of moderate fertility with calciam dominant in the exchange

complex, except for the solodic types. Solonised types have the poorest water

status and the red-brown earths the best,

06 D. F. SMITH

3, Rendzinas and Terra Rossas

The expanse of limestone along the western coast is generally coyered by

a thin mantle of grey-black or red-brown loams and sandy loams, although on

slopes the limestone may be bare. Some other limited arcas of tetra Tossas

occur Where sufficient limestone has accumulated to dominate soil formation,

Many such patches, an acre or two in extent, occur throughout the Kapinnie,

Cummins and Yeelanna districts and have typical vegetation. Accumulations

of calcareous sands and sandy loams also occur in association with the large

expanse of litnestone,

The rendzinas and terra rossas are typically alkaline, quite high in fertility

and have low water storage capacity,

4. The Deen Sands

Areas of calcareous sand occur along the coast and as deep pockets associ-

ated with the limestone (up to 83 p.c. calcium carbonate with a pH of 8-9)

even as far inland as the main railway line near Karkoo.

Deep siliceous sands occur in restricted areas, mainly at Wangary, then

squth aud west of Cummins and in a complex area north of Yeelanna-Ungarra,

Most of these have a pIT 5-8-6-0, and are of very low fertility with low water

storage capacity,

5. Soils Associated with Archaean Rocks

Depending on topography these may be skeletal or quite deep soils on the

mid and Jower slopes, varying greatly in texture and fertility according to

rock type. Some yellow solodie soils oecur,

In terms of soil fertility and water storage capacity this group supply the

most favoured habitats for plant growth and carried savannah woodland veue-

tation.

6. Solonised Brown Soils

South, west and north of Yeelanma considerable areas of these soils occur,

carrying the typical mallee serub with Eucalyptus flocktoniae and Eucalyptus

pileata as dominants, As usual these soils are strongly alkaline (pH 6-5), have

relatively high nitrogen and phosphorus status and total soluble salts of O-1 pe.

Calcium and magnesium contribute almost equally to the relatively high cation

exchange capacity,

CLIMATIC HISTORY

Crocker (19466) and Crocker and Woad (1947) have discussed post-

Miovene climate in Australia, and Smith (1960) has discussed the Eyre Penin-

sula evidence in detail. The Recent aridity would appear to have had a profound

infhence on Eyre Peninsula yegetation (sec later).

Downes (1954) has suggested that present day drought conditions represent

average conditions during the arid periods, ie. ayerage annual raiufall was

down almost to half of the present day amounts. Botanical evidence suggests

that on Eyre Peninsula the reduction was less severe than this— from 20 inches

down at most to 13 inches, Further, the zone of maximum solonisiution on Eyre

Peninsula (the red and yellow soladie soils) is now somewhat drier than Suge~

gested hy him, His principle that high calcium status. markedly reduces mor-

phological change during desalinization of the surface is strongly confirmed.

I )) Ly

LEGEND

1 COD e eaicitis

E, FLOCK TONIAE

E.PILEATA-M UNCINATA,

3 ROSE E_DIVERSIFOLIA

FE. LEPTOPHYLLA

E.ODORATA VaR

ANGUSTIFOLIA

E CLADOCALYX

o CAS STRICTA

£ LEVCOXTLON

12 CAS, STRICTA

M.PUBESCENS

VEGETATION OF 13 M, PUBLSCENS

LOWER EYRE PENINSULA 14 a costa cures

Beyer) 1.2.3.4.

Emme] 12,3. 12, POOMPLEXES

CMT) 2.3.4

“Trans. Roy. Soe. S.A.". Vol, 87.

PLANT ECOLOGY OF LOWER EYRE PENINSULA, S.A. oT

When calefum is low, ay in the siliceous sands and leached lateritic soils even

moderate present rainfall (13-18 inches) has caused the development of

solodized soloneté and solodic soils and vegetation changes accordingly,

VEGETATION

Invrnopuerion

The only previons study of the ecology of Eyre Peninsula was made hy

Crocker (1946a). Only a small percentage of the southern area is still uncleared,

and of this most must have been affected by fire, livestock, rabbits, competition

from introduced species, and other influendes due tu settlement. Distribution

of the original vegetation has been assessed. hy a consideration of relic patches,

old records, opinions of eurly settlers and remaining vegetation along roads, with

allowance where possible for the known inHuence of settlement on the frequeney

or distribution of a species,

Coaldrake (1951) lists depth of sand, water status, presence of massive

limestone and burning as major factors influencing distribution of plants in the

Ninety Mile Plain, and these factors seem to wperate in a very similar way in

this region, Tire has not influenced such large areas at the one time, at least in

recent years,

Kucalypt identifications have been based mainly on the key of Burbidge

(1947) and checked by C, D. Boomsma of the South Anstralian Woods and

Forests Department, Other species have been identified and/or checked by

Us National Herbarium, Melbourne, using Black’s Flora of South Australia in

almust all cases, A set of specimens has been deposited at that Herbarium.

Floristic lists have been compiled ineluding comparisons with related vegetation

units elsewhere, Copies are available from the author,

Noves on InpivipuAL SPecnes

1, Eucalyptus camaldulensis (river ved gum)

River red gum specimens on Lower Fyre Peninsula are generally very

similar in tree size, bud and froit characteristics anf location, to those occurring

elsewhere in Australia. However, there is apparently some hybridization with

Lucalyptus cladocalyx and Bucalyptus lencaxylon such as at Chapman’s Swamp,

five miles west of Wanilla, the hybrids having Jarger fruits than normal, yet

otherwise reasonably typical appearance. This species ig restricted to areas

where soil is moist fo a considerable depth. ie. former stream beds now covered

with secent sediments, or where streams run into acolianite limestone, giving

shallow watertables, It does not occur naturally in the Koppio Hills where L

leucoxylon occupies sites on which one would expect ta find it. The one. valley

necurrence is fust cast of Wanilla, The largest individual area is at Dutton, on

meadow podzolic type soils at the foot of the Marble Range, Seyeral patches,

totalling several thotisand acres, occur at Koolidie Station, on the northern

boundary of the Hundred of Mitchell (PI. 2, Fig, 2), ere I. catmaldulensis

and Callitris propingua form an ecatone on shallow sandy loams over travertine

where a creek Joses ilself under the travertine, giving a watertable at 10-25 feet.

On ridges where the watertable is deeper there is no red gum.

95 D. F. SMITH

3, Rucalyptus cladocalyx

This species is remarkable fur ity discontinuons distribution in South Ais-

truliu, to which its natural occurrence is restricted. It occurs on Kangaroo Tslard

Lower Eyre Peninsula, the Cleve Hills, and the Southern Flinders Ranges, each

oceurrence being on a different type of soil* and Horistically imrelates!, On

Lower Eyre Peninsula it is often depuuperate, and always a twisted tree (PI. 1,

Fig, 1) growing over selerophyllous shrubs on Lateritic soils.

©. D. Boomsma (personal communication) has drawn attention to the fact

that specimens from the Flinders Ranges, when planted on Kyre Peninsula alony-

side local specimens, grow straight and more vigorously, indicating some genetic

divergence.

The Horistic lists compare the E. cladoculyx association with its occurrence

elsewhere (Baldwin and Crocker, 1941; Boomsma, 1946). Only six of the

86 species from the LE, eludocalyx associution ou Eyre Peninsula have heen

reearded in the L. clacacalyy assuciation on Kangaroo Island although some 5

of the 66 have been reported from the Island. Likewise only [1 species are

common to E. cladocalyx stands in both Eyre Peninsula and Flinders Ranges,

but 30 of the 66 are recorded for the Flinders Ranges. ‘Vhus, if the EB. eladecalyx

distribution is due to retreat to give a discontinnous distribution, survival and

some spread, it shows the puzzling feature of fuilure fo have many constant

cimpanions. Lf all species making up an association lurve not an identical

range but an averlapping range, it is possible thal in w severe battle for survival

almeast all companions could be lost. Tt is possible that the prominence of &,

cladecalyx on Eyre Peninsula is due to the absence of Luculyplus baxieri despite

the occurrence of situations where soil and rainfall vonditions appear to he

salable for it by comparison with Kangaroo Iskind where the lower rainfall

limit is approximately 21 inches. Lf FE. Dagleri was presont £. cladocalyx might

be limited to the drier lateritic soils and skeletal ridges, whereas it now occupies

all the peneplain surfaces of the Koppio Hills where yainfall is greater than

16 inches, some slopes and even valley floors. Soils are generally moderately

wel, with reasonable drainage due to slope or the presence of rock fragments

or pisolitic iromstoue gravel. It attains its greatest size on well-drained logs

wear ¥allunda lat. reaching a diameter of three feet and a height of 60 feet,

but is never the large, handsome tree of the Flinders Ranges, Many of the larger

trees have been remuyed and milled for rough farm work.

Near Wanille aid towards: Edilliie patches oveur well out unto the phiiu,

frequently depauperate. The reason for its failure to spread across the plaiu

appears to be related to the degree of water logging. Near the Marble Bunge

and westward to willtin a mile of the coast at Mt. Dutton the tree attains a

reasonable frequency, often mixed with E. camaldulensis, BE. leucoxylon and

E, adorate, but in a few cases as pure stands on lateritig remnants.

The boundaries of its occurrence are offen very sharp. On the south avd

west dhig is apparently due to marked soil changes where the Uavertine-capped

aenianite mantle overlies the laterite. On the east, where the plates laterite

gives way to skeletal chocolate soils on steep slopes and a rain shadow operates,

combined soil und climatic factors determine its margin. At the north-western

linnit the change js still relatively sadden, with depauperate BW. eladocalyx (Ch 1,

Vie, 1) giving way to Lucalyplus incrassete ou the peneplain remnynts but at

fill ove on alluyion lomoine “atypteal savunnaly merging te seleyaphyll forest” { Northeote ane

Preker, 1948). Winders Rages —large Tundsome tree on qnartzitic ridges above [000

fept contour, Savannah woodland (Boomsma, 1946),

PLANT ECOLOGY OF LOWER EYRE PENINSULA, S.A. 99

its northern margin itis a tree of up tu 20 tect in height, Fig. 5 indicates some

of the relationships of E. eladecalyx and ether evcalypts north of Yalhinda Flat.

Thus on Eyre Penisnla dense stands only occur on laterilic or related

soils and never uaturally on limestone soils, which is interesting, in view of the

widespread and successful planting of it on such soils elsewhere. Its ecological

limit may he related to snbsoil or surface drainage and/or caleium carbonate

enrichment in some way, perhaps operating only on scedling establishment and

survival, as plantations elsewhere are usually planted as seedlings and watered

the first year. To the north where its margin cannot be explained in edapho-

climatic terms, it may be that iv spreading from a centre of survival it has only

reached this point. Further spread wendel he prevented by grazing as although

young trees grow densely after firing they are easily grazed vut,

3, Eucalyptus leucoxylon, var. macrocarpa

E. leucoxylon oceurs extonsively with £. odorata, but no hybrids have been

noted on Eyre Peninsula which is of interest in the light of the observations

of Pryor (1955), who records hybridising near Adelaide.

i. leacoxylon is Found on ullavial soils of relatively high fertility on yalley

floors and lower slopes where moisture penetration is good, yet severe and

prolonged waterlogging does net oecur, Beksw 18 in. rainfall it is present only

along creeks, e.g, it follows the Ungarra Creek ont onto the plain into a 14 in.

rainfall. It appears araund the Marble Range where coarser sediments hyve

been deposited. Its occurrence east of Yeclanna at Brooker where wind-hlown

siliceous sands juve piled up in a drainage line is in a habitut usnally ocenpied

by kL. camatdulensis.

4, Eucalyptus odorata

Both E. odorate and L. odurata var, angustifolia are widespread almost

throughout the area under discussion,

(a) EE. edavata

This tree Sorm appears to be very similar to other oecurrences in South

Australia, lt is the sole dominant on the most fertile soils ~ red-brown earths,

chocolate skeletal soils of the wpper slopes and a wide belt of fertile transitional

red-brown earths froin Lipsou throuvh Stokes to the railway line at Cockaleechie.

Outliers gecur at Mt. Isubella, north-east of Yeelanna, surrounding an onterop

of Archacan rocks, near Mt. Hope and near the Marble Range. Rainfall is

always 16-19 inches and soils are always relatively fertile and well drained.

There is a lansition through an ecotote to 2. leucoxylon where drainage is

inferior us in the valleys in the southern ilk of the Koappio Hills.

(h) &. oderata var. angustifolia

The form of this variety is quite constant, being 6-12 feet high usually in

clumps. It ovenrs on heavier textured, more waterlogged patches than the

tree aie within the same overall climatic limits. Tt is difficult to lall by burn-

ing and ploughing so is now conspienans where it may not originally bave been

a praminent meniber of an association,

5. Enecalyplus belriana

“. behriana as a mallee form is scattered widely but generally infrequeutly

through the mallee formations on the Jower western slopes of the Koppio Hills

fram Wanilla to Yeelanna, and odd individuals are found along drainage lines

400 D. F. SMITH

furtlier west. Specimens fit into the general type description of Blakely (1955).

heing conspicuous for their very broad leaves (up to 2 in.) and terminal pani-

enlate inforescence,

Rodger (1953) suggests that the typical habitat for this species is on dry

soils, frequently calcareous sandy loams and sands. Howeyer, on Eyre Peninsula

E, behriana is more usually found on heavy grey silty loams with 17-19 inches

OF rainfall, fitting more the habitat ninge described by Litchficld (1956) fur

the Counalpyn Downs.

Due east of Cummins (PI. 2, Fig. 1) Ef. behriana occurs as a co-dominant

with E. odorata yar, angustifolia on an area of grey silty alluvium with poor

subsoil drainage. ‘Vhis is the only recorded occurrence of it as an association

dominant in the area and provides a link with Victorian observations where

Rodger (1953) lists 2. behriana us oimmonly occurring with Kucalyplns frutice-

terum (considered by Borbidge as being synonymous with i. odorata var.

angustifolia) and E. viridis, a closely allied member of the Odorata complex,

6. Eucalyptus calcicultrix

Compared with other locations, E. culcicultrix is easily identified on Byre

Peninsula. It is restricted to the western side of Lower Eyre Peninsula, usally

vn deep calcareous sands and sandy loamy over limestone in undoubtedly very

dry habitats.

7. Eucalyplus huberiana

On Eyre Peninsula this species is not the handsome forest tree of Other

parts of Australia, but has curved trunks, giving a spreading, even stragpling

appearance, It occurs in two small patches some 15 miles apart and may ut

be indigenous. The main one consists of a dense clump of trees near the old

Mikkara homestead, south of Port Lincoln, with odd tees withm two miles;

the second occurs west of the town uear Big Swamp, and adjacent to the old

couch road, consisting of some 20 trees. Bearing, in mind their rapid regenera-

tiow after firmg, both oecurrences could have been derived from one or two

trees planted near an old homestead and a coach watering point, On the other

hand. location near an old homestead is not necessarily evidence of the trees

having been introduced. In an area of mallee a yroup of larver trees would

hea likely site for a homestead, especially as underground water could be found

under the travertine layer.

Climatic considerations could support a natural occurrence, as the climute

would be similar to its habitat elsewhere, with moderate temperature and te-

Jiable rainfall. Although there is a vencer of travertine at the southerly @ccur-

rence, roots would be in moist soil at reasonable depth in both cases. The

two groups of trees are on opposite sides of a taungue of travertine which covers

much of the area suitable climatically for its growth. Thus it is not surprising

that its distribution is limited. Mowever, there is some doubt as to hes it

survived the recent aridity, and subsequently came to pceupy its present situa-

lion, Tt could be expected to have survived in the Koppio Hills also and to

have expanded cunsiderably more than it has with a recent increase in rainfall.

All things considered, planting by curly settlers scems likely.

8. Eucalyptus diversifolia

As elsewhere in South Australia, the aacurrence of E. diversifolia is closely

related to travertine limestone formations. Lt is the sole tree dominant aver a

sermb on limestone ridges near Kapinnie and Lake Hamilton.

PLANT ECOLOGY OF LOWER EYRE PENINSULA, S.A. 10L

9. Lucalyptus incrassata

Specimens vary in size of fruit, ribbing of fruit, and coarseness of foliage,

but there appears to be less local variation than recorded by Coaldrake (1951)

in the Upper South-East of South Australia, and within this region it grades.

into 1, pileata rather than B. anceps, French: (personal communication ) has also

verified the forms found here as L. inerassate var. costata (Burbidge) with some

tendency to the even evarser var, angulosa (Benth), Certainly Burbidge’s com-

ment that these two are points in a serics is borne out, No attempt has been

made to separate them in this study, the specific name only being used.

E. incrassata is the most common mullee on solodized solonetz soils and

the sballaw secondary laterites on the Wanilla plain. In a few cases it has

been found as a dominant on deep coastal siliceous sand dunes.

On the Cummins plain where “ripples” of siliceous sad form a mosaic on

the otherwise heavy clay flood plain, EF. incrassata follows closely the sand

under which solanization has been most marked, Its tolerance fo winter water-

logging and summer dessication apparently enable it to maintain this distribu-

tion, Its tolerance to salinity (or physiological dronght) allows it to persist

further into some saline situations than other mallees.

Several trees occur on Boston Island near Port Lincoln. These are par-

ticukirly coarse forms, haying large, prominently-ribbed fruits and thick leaves.

10. Hucalyptus pileata

This and other members of the dumosa group present show considerable

variation. E, dumosa as described by Burbidge. (1947) is absent, but E. pileata,

which is extremely widespread and often dominant, is similar in many ways,

E. anceps (or an allied form) is common also, and E, rugosa and E, conglobata

have a more restricted distribution, )

LE. pileata in its most common form matches the deseription of Burbidge.

However, there is much variation in the fruits —small with faint ribs, smooth

fruits, and Jarger fruits with more prominent ribs all occur. These last tend

towards Fi, incrassata. Pedicel length also varies, grading towards F, anceps:

FE. pileata is widespread with E. flocktoniae in typical mallee formations on soils

with broken nodular limestone in the profile and often on the surface.

Its rainfall limits appear to be 14-18 inches, being replaced by FB. gracilis

on the dricr side of its range.

Lt Eucalyptus anceps

Burbidge (1947) discusses the difficulty in differcntiating this species from

E. pileat, E. rugosa aud EK, conglobata. and in this study quite a range of

material has beeu grouped as E. anecps. Certainly the presence ar absence

of a pedicel is not a good diagnostic character, and several pedicellate forms,

too small and plain of fruit for E, pileata, have been included. The species is

quite widespread at low frequency but never dominant.on Lower Eyre Peninsula.

13. Eucalyptus rugosa

E. rugosa ist seasonable constant member of the dumosa group. It reaches

its greatest frequency near Port Lincoln on or near the edge of the aeolianite

limestone.

102 D. F. SMETIL

13. Eucalyptus conglebuia —

According tu Blakely (1953), E. vonglobata only occurs in Western Aus-

tralia and South Australia and im the latter only on Eyre Peninsula and Kan-

gavoo Island. On the Eyre Peninsula mainland it is seattered through other

mallee associations near Port Lincoln, essentially as a stunted malle, often on

lateritic soils. Tlowever, the absence of competitors and firing appear to have

permitted it to develop into a dominant tree up to 40 feet high on Boston Island,

Where it forms an attractive woodland (PI. 2, Fig. 3). Unfortunately, recent

burning has destroyed many individuals—its peeling lower bark and bulbous,

hollaw butt make it fire-sysceptible. It is also recorded on Taylors Island

further south.

4. Eucalyptus brachycalyx

This also seems a reasonably fixed type except for the variety chindoo, It

is not ecologically important, occurring at low frequency in the drier mallee

serub.

15. Eucalyptus flocktoniae

Field experience suggests that in certain localities this and lM. oleosa form

a complex, with intergradig of material from eveu small areas, French (per-

sonal Communication) has confirmed this view. However, in many other areas

on Lower Eyre Peninsula quite distinct E. flocktoniae can be identified, and in

others quite distinct E. oleosa and various varieties, especially var, glauca.

Burbidge (1947) considers that E. flockteniac is a link between E. oleasa

and the Western Australian species E. torquata, and this Eyre Peninsula obser-

vation confirms this, although such difficulties have not been reported -else-

where. C. D. Boomsma, on examining material collected hy the author, has

suggested that E. flocktoniae and E. olevsa arc more directly related than was

earlier thought (Boomsma, 1949).

Both species, and all intergrades, are always true “mallecs” in habit oecur-

ring on grey and brown calearcous loams and sandy loams, frequently solonised

—typical “mallee” soils, E. oleosa in its strict sense generally oecurs wilh E.

gracilis in drier areas with rainfall below 14 inches per annum, E. flocktoniae

with B. pileatw is found on similar soils in wetter areas, as near Cummins where

n. fe is quite a distinct species, matching the description of Burbidge

(1947).

16. Evealyptus oleosa

On Lower Eyre Peninsula specimens af FE, oleosa var. glauca wre particu-

larly common with much true E. oleesa and a full range exists in some localities

from E, oleesa through var. glauca to E. flovktoniae. One such series was col-

lected over a square chain area near Mt. [lope. Yet, curionsly, over much

of the region the species and its yariety are quite distinct from each other and

from Ef. flocktonide.

This is, of course, the widespread characteristic mallee of the arid zone

of South Australia, and is only important in the drier north-east corner of the

area under study.

PLANT ECOLOGY OF LOWER EYRE PENINSULA, 8.A, 103

17, Buealyptus leptophylla

Over most of its occurrence this species matches the description of Bur-

bidve (1947), but forms with thicker fruit walls and wider leaves. cause some

confusion, It is suggested that some hybridisation with E. gracilis nay have

occurred. The greatest variation in this species occurs in the Hd. of Mitchicll.

E. leptophylla is widespread, especially with E. inérassita, ocenrrmg on

slightly moister soils than pure stands of the latter.

18. Eucalyptus uncinata

Although specimens have heen identified as l. unetnata, they could quite

sasily have been named shortly pedicellate E. leptophylla.

19, Euculyptus gracilis.

This species is rarely confused. Some forms appear to grade towards L’.

leptophylla, but if buds or flowers are present, it can be distinguished on

stamen characteristics. A forrn found only on Boston Island has a very small

cap, much narrower than the fruit, and foliage resembling E. largiflorens. 1.

gracilis occurs widely on solonised brown svils with moderate to heavy limestone,

varying in texture from clay loams to sandy Joams and usually receiving less

than 14 inches average annual rainfall.

20. Eucalyptus calycogona

E, calycogonn appears to grade completely into the coarse form, var. stuf-

fordii, Tt is quite widespread, especially with E, flocktoniae-E,, pileafa around

Cummins. On some shallow red clay loams near Ungarra it is occasionally the

sule dominant oyer small areas,

31. Eucalyptus landsdowneana

This member of the odorata complex was not widely collected, being re-

stricted to the Port Lincolu-Wangary urea at low frequency.

22. Callitris propingua (Native Pine)

“Pine” does not aconr extensively except in the north of the region on

ealearcous sands und sandy loams near Koolidie. It is much sought after as

tenice posts and has been heavily ent over, Further south soils are not par-

ticularly suitable for its growth.

23. Acacia pycnantha

Of the many species which have been introduced and wow have a wide

distribution the only tree species is A. pycnantha. Claimed to have been intro-

duced in the 1880's, it is now widespread above 17 inches of rainfall on soils

ranging from the sandy Jateritie types of the hills to the heavy clays near

Cammins. Ou the former it may become a secondary dominant after scrub

burning,

94. Nanthorrhoea tateand (Yaoor )

Yaeeus oveur throughout the #, cladecalyx woodland of the Koppiv Hills

(ineluding some soils — for instauce, skeletal slopes, on which E. cladocalyx dues

not grow) and throughout the Wanilla area. In the latter it extends beyond the

E. eladoealyx association into the E. inerassata heath at least as far north as

Kapiinie and inland io about six miles west of Cummins, It is. ahways on

sandy soils with rainfall usually aboye 17 inches, but perhaps slightly less in the

Koppia Hills.

THR PLANY COMMUNITIES

The general relationships of the plant communities identified are shawn in

Figs. 2, 3, 4,5, in Table 1, .and in the doristic lists.

SMITH

D. F.

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106

D. F. SMITH

EXPLANATORY NOTES FOR FIG, 2

General description of |

country

Soils

Vegetation dominants

. EL-AW. section

» NLA. W.

N,-4, section

through

Cummins

through Mt.

Greenly anc

Tumby Ray

ction through}

Koppio, Stokes

and Cngarra

1. Undulating acolian

travertine limestone

2, Mixeil gentl: slopes ane

SWAIPY HOAs

3. low Lying swampy area

subject to flaading

Pod. Bhghthy dissected

lateritic plain

Outwash fan and plain

from dissection of arew

to the east. Poor

drainage

6, Undulating area, rises of

travertine liméstone

7. Rising land towards

Yeelanna

1. Steap slopes of Mt.

Creenly :

Bed of Lake Greenly

Northern slope of

Marble Range

Wide drainage lines |

- we

5. lat outwash plum often

erab-holey and water- |

logged

6. Disseetod slopes

7, Peneplain surface

8. Valley slopes

9, Peneplain surface

10, Deeply anil sharply

dissected :

Gonthy sloping outwash

plauwi

It.

1. Undulating aoolian

travertoe limestone

2, Big swamp bagin

3. Slighthy tilted shallowly |

dissected laiteritie

peneploin

4. Dissected. often steep |

slopes of Vou River

Valley

Slightly tilted, more

sharply dlissectert

lateritic peneplain |

6. Outwash plain |

7. Unodulating

Shallow rendazinas and

terra. rossas

Some calcareous sands,

rendzings and peaty

soils

Rendzinas and shallow

peaty soils

Lateritic pouzols

Red brown carths, grey

soils of heavy texbura,

solodie soils, and mallee

sails

Solonisecl brown soils,

somo Lerra rossas

Red brown earth of

heavy texture

Skeletal

| Stony and lateritie podaols

Alluvium and solonschals

Grey soils of heavy Lexture,

some red brown. earths

Variable stony podzols

Lateritice soils

Vanable stony loaims anil

alluviel sotks

Lataritic

Skeletal

Red brown earths

Shallow rendzinas, terra

rossas, and some

calcareous sands

Peaty soila on tvinge

Lateritic podzols

Variable loams, usually

stony and podzolised.

Some skeletal

| Lateritic podzols

Miuvium anil red brows

earths

Real lateritie loarus, and

red brown carths

O, stricta, M, pubescens,

savannah woodland

C!, stricta, M. pubescens,

HK. iliversifalicr,

Lh. caletoultrix

| Cutting grass and rushes

BH. tnerassata, heath

. pileata, Ei, flock-

lone, B. dierasaeta,

mallee serub and

hroom)ush

H. wiledta, Li, flack

tonioe, BE. diversifolia,

seruh

EL pileata, be. flack-

tonwre

OC. striety,

MB, cladocealyae, hi.

PREPUSSCUleL

AM. pubescens, Ghania

trifida, Cladium filan

E, pileata, f2. flack-

toniae, BE. inerussala

E. odorata, C. stricter

E. eladocalye

HK. odoritie, BE.

Teucoailor

Ei. clhadocalys

| Cl stricta

Hi. adorate

Cl, stricta, AD. prshescens,

E, diverstfolia

' BE, coomoatidatenais

H, eludoculys:

E. cladeculyx, BE. ndorata,

B, leacow yur

Ki. eladocalyv, E.

inemusasate

E, leucowiHon, EB.

olorata, FE. piterits

K. flacktonive

PLANT ECOLOGY OF LOWER EYRE PENINSULA, S.A. LOT

1000 FEET

x 2 3 4 5 6 7

Fig, 2, Diagrammatic cross-sections through lower Eyre Peninsula.

a, North-south through Cummins.

ly, East-west through Mt, Greenly and Tumby Bay.

c. North-east-south-east through Koppio, Stokes and Ungarra.

A. Tae MaLirr

(1) General

It is possible to recognise certain basic associations in the mallee, especially

in the less complex areas to the north, and these also appear in Lower Eyre

Peninsula where soils are similar, A number of associations and types occur

as an edaphic complex, more or less as suggested by Crocker (1946a). Some

revision of the eucalypt classification has occurred since his work (Burbidge,

1947; Boomsma, 1949) and it is clear that his E. dumosa is now generally

classified as E. pileata, and his E. angulosa as E, incrassata. Eight reasonably

108 D. I. SMITH

distinct and consistent mujor units of mallee vegetation have been recognised,

They are:

a. E, oleosa-E. gracilis association,

b.. E. inerassata-E. leytophylla association.

i. E. incrassata~Melaleuca uncinata type.

it. I. leplophylla type.

iii, I. inerassata type.

e. E. flocktoniae-E. pileata-Melaleuca uncinata association,

d. E. diversifolia association, —

i. E. diversifolia-E. caleiculirix type.

Their relationships are shown in Fig. 3.

The vegetation pattern is extremely complex on such areas as the Cnmmins

plain where variations in calcium carbonate content from quite massive trayertine

lo faint marl, in drainage from free to waterlogging, and in siliceous sand. cover

(and hence degree of solonisation) from 9 inches to none may all ocenr in

various combinations within a few acres.

Another unit of vegetation which could be mentioned here is E. conglobata

woodland. [t occurs as 4 mallee less than 10 feet high near Port Lincoln on

the mirgin of the travertine and Jaterite, and on Boston Island it forms a

woodland usually as a tree with one trunk, but a bulbous base not unlike 2

tatllee,

(2) Individual Communities

a. FE. oleosa-L. gracilis Association.

This association is quite widespread on Eyre Peninsula, especially around

Cleve, Kimba and Wudinna, obviously being more tolerant to arid conditions

than any other mallec association in this region. In the area studied it is almost

limited to the drier east coast region with less than 14 inches of annual rainfall.

Soils are usually red-brown sandy loams with lime rubble or travertine at

8-11 inches, often having free surface limestone, and best described ay sandy

solonised brown soils. Above 14 inches of average unoual rainfall it occurs

only on very light-textured soils, as near Mt, Hope where it is intermixed with

the E. diversifolia and E. flocktoniae-F. pileata associations over a small area.

Tris association is usually a mallee scrub with a rich under-storey of shrubs

(especially after burning), the most common being Melaleuen uncinata,

Rhagodia crassifolia, Lasiopetalum behrii, Acacia gillii, A. spinescens, Pimelea

dichotoma, Dampiera rosmarinifolia, Loudonia behrii, Didiscus ornatus, Amyema

miraculosa var, melaleucae, Dodonaca hexandra, Eutaxia microphylla, Halzania

eyanea and Dodonaea baueri.

bh. I. inerassata-E. leplophylla Assceiation

The balance between codominance of the two eucalypts and individual

dominance is a very delicate one, The association occurs in areas of solonised

soils with a mantle of siliceous sunds or areas of shallow laterite profiles. E.

incrassaia is apparently very resistant to both drought and waterlogging, with

I’. leptophylla less resistant to drought.

On deeper sandy areas, up to four feet or more in depth, E. incrassata

eecurs as the sole tree dominant, or with an odd tree of E. diversifoliq. E.

PLANT ECOLOGY OF LOWER EYRE PENINSULA, S.A. 109

leptophylla is more evident when sand is less than nine inches, being co-

dominant with E. inerassata and M, uncinata, On wetter flats with a few inches

of sand If. leptaphylla may be the sole dominant.

On sandy lateritic profiles west of Cummins near the lakes, E. incrassata

and E. leptophylla form an open mallee heath formation, with a rich under-

storey, Melaleuca decussuta, Wibbertia strictu, Grevillea ilicifolia, Chetranthera

linearis, Hakea cycloptera, Hibbertia sericea var, major, Baeckea behvii, Pul-

ienaga trinervis and Spyridwm vexilliferum are the most common slirnhs.

Xanthorrhoea lateana is present, especially Lowards the south,

On the shallow lateritic svils near Wanilla a very stunted form of I.

incrassala (3-5 feet high} oceurs with M, uncinala and with E. leptophylla pre-

sent on moister soils. £. inerassata also Oecurs on the dry tops of the divides in

the northern Keppio Hills, replacing E, cladocalyx.

The under-storey on the Cummins plain is discnssed jointly with that of

the E. flocktoniae-E. pileata-M. uncinata association.

c. E. flocktoniae-E,, pileata-M. uncinata Assoviation.

This association is very widespread on solonised brown and grey-brown

or red-brown Joams with heavy limestone rubble in the profile and frequently

with surface stones, Surface texture and colour varies considerably from loams

to clay Joams and clays. Limestone may be so heavy as to form massive ridges,

carrying 1. diversifalia, especially between Cummins and Yeelanna. In the wet

hollows of the drainage Jines near the hills. the association is replaced by E.

odorata var. angustifolia, a whipstick mallee. Where siliceous sands or lateritic

profiles occur FE. incrassate replaves it and where sandy solonised soils occur the

Ki. aleosa-B. gracilis association is dominant.

Associated eucalypts are E. leptophylla and E, ealycogone, which is almost

2 dominant on some sites, The under-storey is quite rich, with much inter-

twining, Cassytha melantha. Low acacias such as Acacia microcarpa and A,

acinacea, and Melaleuca uneinata are frequently prominent, with also Daviesia

pectinata, Eutaxia microphylla, Lasiopetalim behrii, Bueekea crassifolia, Hakea

cycloptera and Hibbertia stricta. A wide yvaricty of orchids oecurs in season.

2c DA 4A

— Tl

SILICEOUS jp

SAND LIMESTONE CALCAREOUS SAND

Fig. 3. Relationship of mallee conmiunities.

\, #. oleesa-f, eracilis association,

_tnerassata-&. leptowhylla association.

A. 2, lacrassata-M. uncinala type.

RB. 2. leptaphylla type.

C, E, incrassata type.

E. flocktoniae-E, pileuta-M. uncinafa association.

4, ¥, diversifolia association,

A. E. diversifolie-E. culgicultrix type,

110 D. F. SMITH

Most of these undershrubs persist even on the lighter soils where E, ineras-

sata and 1°. leptophylla are the dominant trees, with perhaps more Dampiera

rosmarinifolia, Dillwynia hispida and Prostanthera microphylla. Jn wet hollows

Callistemon macropunctatus (svn. C. rugulosus), Lasiopetalum behrii and

Melaleuca acuminata are the most prominent shrubs.

Where travertine Jimestome occurs in the soil at shallow depths the chief

shrubs are Acaeia spinescens, Lasiopetalum behrii, Grevillea ilicifolia, Goodenia

geniculata and Correa veflexa,

d. EF. dicersifolia Association

Although this is frequently open it may pecur as dense whipstick mallee

with no under-storey. Its occurrence is virtually restricted to travertine areas

with very shallow soil coverings, The limestone is rarely thick and usually

crucked. Many of the shrinbs are those found in malleo serubs nearby, with

more of the high ramfall sclerophyll species near Port Lincoln.

‘Towards the western coastline where calearequs sands have accumulated

om the travertine 2, diversifolie and BE. caleicultrix occur together with or with-

gut serub elements.

e. £. convlobeta Association

The association is Only found on Boston Island (PL 2, Mig, 3) and perhaps

Taylors Island. Associated eucalypts are DE. vracilis und E. ineresseta and a few

sclerophyllous shrubs — Anthecercis anisantha, Pimelea stricta and the fern

Cheilanthes teniifolia, Others may have been exterminated by sheep grazing.

B. SAyYANNAH WoopLAND AND SCLEROPUYLT. SOKUB

(1) General

It is frequently dilficult to determine the original extent af sclerophyll

serub, as large areas, through grazing out of the wnder-storey, may now haye the

appearance of woodland. Of the encalypts present, BE. odorata and 1. caniil-

dulensis are possibly the only two whieli formed a truce savannah woodland, the

former as a single dominant and with LE, leucoxylon on alluvial soils in the

Koppio Hills and LE. camafdulensis in isolated small arcas especially near Wan-

garv and Mt. Dutton. £&, cladacalyx is usually the dominant in a dry sclerophivll

scrub, and where it now appears ay a savannah woodland the shrubs have

apparently been climinated by grazing,

(2) budivicuel Communities

ae L. eludecalyx Association

As a sclerophyll sernb this ocenrs on residual Jateritie podzols on the

phiteau remnants of the hills (PI 1, Figs, 1 and 2) and alsa extensively near

the Marble Range. Its margin is sharp (see notes on fudividual species).

At its northern limits E. eledocalyx torms an ecotone with I, incrassala

over a dense mallee sernb. Deaviesia polyphylla aud Pultenaea teretifelia form

local socielies, Xeanthorrhova tateana, Spyridium vexilliferum, Hakea vuecasi,

H. cycloptera, Astroloma conostephioides, Grecillea ilicifolia, Hibbertia stricta,

Lusiopetalum. behrii asd Melaleuca uneinata are the most common shrubs. Trees

al Casuarina siicia and Acacia pycnantha are present.

Near Wanilla on the edge of the peneplain and down the slopes on normal

lateritie profiles. £. cladocalys forms aw canopy over a dense and varied serub.,

Xenthorrhoca tateana wud Acacia rupicola ave extremely common, while Baeckea

PLANT ECOLOGY OF LOWER EYRE PENINSULA, S.A. Il!

belirii, Daviesia brevifolia, Grevillea ilicifalia, Astroloma hnanifusum, A. cono-

stephioides, Melaleuca uncinata, Hibbertia strieta and Fxocarpus sparteus are

less so, with many other aninor species.

On the shallow gneissic stony loams of the slopes the understorey is rela-

tively poor, and Xanthorrhova luteann may form a society, Casuarind 5! neta

is also more common on these soils,

b, E. odvrata-Casuarina stricta E:daphic Complex

(i) 1. odorata as a pure dominant.

As a tree form, E. aderata occurs almost as a pure dominant in many places

on lower Eyre Peninsula, The edaphie and climatic factors controlling its dis-

tribution have been discussed in the notes ou individual species. Cround

eover is usually Danthonia semiannularis aid various Stipa spp. with some

Dianella revolula and Bulbine semibarbata,

On the deeper red-brown earths of the Cockaleechie Valley, mallee sernb

merges into an BE. edarata woodland, The transitional stage contains woodland

and mallee serub elements — Dianella recoldta, Bulbine semibarbata, Enchylaena

lomentose, Acacia acinacea, Gassinia complanata, Dodonaen baueri, Muchlen

beckia adpressa, Thrypomene micrantha, Lostopetalum baneri, Eutaxia micro

phylla and Diviesia pectinate being most ohyious,

i. odorata also occurs in a Whipstick roallee form and its ecological rela-

tionship to the tree is one of the most puzzling features encountered. — [ts

habitat has bewn discussed earlier (sce notes on medividual species). Lt is rarely

a dominant in an association. and does not seem to grade into the tree farm.

A variety of shrubs may he present from surrounding scrub,

(ii) B. odlorata-Casuarina stricta Savannah Woodland,

Where soils ave shallower, steeper sloping and apparently drier, E, odorata

ix Increasingly mixed with Casuarina stricta, which may completely replace it

on very slecp skeletal soils, Along, the eastern scarp of the Koppio Wills ©.

stricta appears to have been the sole tree dominant but in several places — ils

near the Burrawing Mine, west of Turmby Bay — EB. edorafe oceupres some sit

prisinvly steep situations,

(iil) £. ederata-E. lereoxylon Association

This association oceurs on all the well-drained alluvial sites in the Koppio

Hills. and also near the Marble Range, Allhough FF, odorata may he almost

absent in a few localities, itis prohably better to consider the presence of both

as an association rather than an ecotone of F. leucoxylon and E. odorata associa-

tion, ‘The association reaches its maximum development ncar Yallunda Flat,

where both members are found well up the slopes. This is one of the few cases

where remnants. of apparently anboredae” veovlation were not seen. Being on

fertile, well-watered soils, much of this association was cleared soon after scttle-

ment. Tt was apparently a savanmah woodlund.

(iv) 2. odorata var, angustifolia-E. buhriana Association

Although EB. behriana can he found sedttered over a wide area on grey

silty Joams in and west of the Koppio Hills, it only reaches dominance in a

few plices. Kast of Cummins where a number ot creeks wive a considerable

area of His type of soil, E. odorata var, anvustifolia and E, behriana are co-

dominant. This vegetation type appurently extended over some thousand or

inare acres, Shrulas may be present,

112 D. F. SMITH

c. £, camaldulensis Savannah Woodland.

At Dutton and Wangary E, camaldulensis savannah woodland covers a few

thousand acres on areas of alluvium and meadow podzolic soils, Patches also

occur in isolated areas throughout the plain where there is deep water pentra-

tion of the soil. Otherwise E. camalidulensis occurs in an ecotone with E. diversi-

folia where water fows into or under the travertine. (See Pig. 4,)

Mallee _

associations

Cas.stricta

E derverstfolta

— “

“Sots ~

“tere

E -ealcicultrix | carwldulensié

Edtversifolra (f i

“ aA H

_— a J

| |

| 1

\ |

Caleareou sl

| Older land

CROSS isands | surface with

SECTION ! drainage lines

Travertine e »

capped aecolianite

Pig. 4, Location of Bucalyptus cumaldulensis in relation to limestone.

d. Casuarina stricta-Melaleuca pubescens Savannah Woodland.

Although a common association on npper Eyre Peninsula this only occurs

in a strip along the west coast from near Port Lincoln to Lake Hamilton on

rendzinas and terra rossas. Af. pubescens is present especially on lower slopes,

being rare on skeletal rises. Towards Port Lincoln this associution is inter-

spersed with E. diversifolia mallee scrub. Large areas arc completely devoid

of trees, only rotting trunks indicating the former dominants. . stricta is a

short-lived tree and rabbits and sheep have prevented regeneration.

Principal native grasses appear to have been Danthonia senviannularis,

and Stipa erémophila. Spinifex hirsutus is very common near the coast and

Nicotiana glauca (tobacco bush) near Lake Greenly,

This association also oceurs aloug the coast north of Tumby Bay, where

shallow loams have formed over Archaean rocks. Much of this Jand has heen

cleared, and it is difficult to tell whether the original vegetation contained

much M. pubescens, or was pure C. stricta woodland. Lomandra lencocephala

remains common on skeletal slopes to the north and Xanthurrhoea tateane to the

south.

e. Castarina stricta

On skeletal soils on the steep faces of such hills as Mt, Dutton and Mt,

Hope, Casuarina stricta appears to have always been the sole dominant. [ts

relationship with E, odorata on the eastern fringe of the Koppio Hills has

already been described.

f, Melaleuca pubescens is often the sole dominant on shallow soils near the

edges of salt lakes.

PLANT ECOLOGY OF LOWER EYRE PENINSULA, S.A. 113

C, Ecotonus

Because of the complexily of the soil pattern, the dependence of vegetation

on soil characteristics, and the gentle climatic gradients, ecotones frequently

occur, solue so frequently as to be given association rank, ee. E, odorata with

E, leucoxylon and E. odorata with Casuarina stricta, This is. of course, to be

expected where several species have habitat ranges which differ only slightly.

Because the margin of the #, cladecalyx scrub is often sharp ecotones between

it and the mallee are not as common as might be expected,

Main ecotoncs are —

(a) E. eladocalyx-E. incrassata-E. leptophylla.

This oceurs uear the north-western margin of the sugar gum where E.

inerassata is present on the drier Jateritic soils of the peneplain in sparse and

depanperate stands of E. cladocalyx.

(bh) E. eladocalyx-E. odorata yar. angustifolia.

Just below the breakaway edge of the lateritic capping of the perieplain

there is frequently a band of this ecotone. The presence of Jateritic gravel and

stone, and soakage from the peneplain apparently make ecesis of both possible.

Fig. 5 shows this relationship.

This ccotune is undoubtedly an expression of the gradual transition from

dry skeletal soils (carrying Casuarina stricta) to the deep, well-drained, red-

brown Toums ut the foot of slopes or chocolate loams of the gentler mid-slopes

both of which carry EF. adorata,

(d) 1. diversifoliu-Casuarina stricta-L. camaldulensis.

As already described these form an ccutone at the edge of the travertine

(Fig. 4), the L. diversifolia and ©. stricta bemg adapted to surface conditions —

shallow, dry rendzinas —and the EF. camaldulensis persisting because of under-

ground water at shallow depths.

Mig. 5. Vegetation of the dissected peneplain and slopes.

NM. cladocalyx scrub on pencplain.

LE, claclacalyx-E, odorata var. angustifolia scrul) below breakaway edge.

E, odorata woodland on yariable stony lowms on slopes.

E, odorata-E, leucoxylon on valley Hoor alluvium.

See

M4 D. F. SMITH

(ev) BK, camaldulensis-Callitris propingua.

This ceotonc at Koolidic Station is due tu similar conditions to (d) ahove,

with Callitris propingua on deep sandy soils overlying limestone with a shallow

wautertable.

D. DISCUSSION

(a) Relationship of the Plant Communities.

The structure, range and relationship of the plant communities is stim:

mourised in Table 1. The structural formulae are based om the work of Wood

(1960). Figs. 3-5 indicate other aspects especially the effect of local changes

in svil Factors on vegetation.

(hh) Ecological Significance of Species Distributions.

Because of arid conditions prevailing across northern Myre Peninsula, the

mister southern portion carries a flora which is completely isolated from that

of similar climatic zones in South Australia and Western Australia.

Lt seems likely from a consideration of climatic data and soil type studies

that rarely, if ever, would a species from lower Eyre Peninsula have a continuous

distyibution through this northern part to some other occurrence. Mean annual

rainfall falls below 10 inches around Whyalla and on the Nullarbor Plain,

Crocker (1946a) descrihes the vegetation of this region —an Acacia sowdenii-

Casnarina lepidophtoia edaphic complex with saltbush and bluebush, typical of

much of the north-west of South Australia.

Thus most species found in the region here described are separated from

their main oceurrence, Wood (1930) has eomparcd the sclerophyll vegetation

of Kangaroo Island and the adjacent peninsulus, and found only 10. recorded

species to be endemic to Eyre Peninsula. Crocker and Wood (1947) have

suggested that a period of avidity during the mid-Recent, apparently sudden

in onset, caused a widespread destruction of vegetation, a retreat to centres

of survival where steep climatic gradients enabled the relatively slow-moving

vegetation units to keep pace with climatic change, and the initiation of changes

in soil morphology. This last is fully discussed by Crocker (1946b), Crocker

and Wood further suggest that a slightly moister present climate has permitted

expansion from these centres of survival, but onto a soil mosai¢ unreloted in

many ways to that preceding retreat. Their list of probable centres of survival

inchides the Koppio Hills and Cleve Hills on Eyre Peninsula, the Guwler Ranges

across its northern boundary, Kangaroo Island, and the Mt. Lofty and Flinders

Ranges on the mainland, They also quote examples from Eyre Peninsula veye-

tation to support their arguments.

Table 2 shows the oceurrence elsewhere of the eucalypt species recorded

gr lower Eyre Peninsula. [n most cases varieties have been grouped together

under the specific title. The groupings of species in brackets according to the

relationship suggested by Boomsma (1949) indicates the strong development

of certain groups,

From the consideration of present topography and rainfall gradients it és

apparent that of the surviyal centres suggested by Crocker and Wood, Mt.

Lofty and Flinders Range wonld be favourable to high rainfall species ind

variable in habitats, Kangaroo Island would be slightly less favourable and

less varied, Eyre Peninsula still less, and Yorke Peninsula yery poor. High

PLANT ECOLOGY OF LOWER EYRE PENINSULA, §.A,

rainfall country eucalypts, even if they did occur on Eyre Peninsula, wonld he

forced south, then extinguished. When rainfall increased again they could not

recolonise unless powers of long distance disperston were high,

115

If we assume that the past climatic range of the species was as it is today,

we can predict which species would have survived.

of higher rainfall eucalypts, the rainfall range given for various areas, and the

TABLE =z

Table 3 lists a number

Occurrence of Lower Eyre Peninsula Eucalypts in other regions in South Australia

\ Upper

i South

Elsewhere | Flinders | Mt. Lafty Kast and

ou Byre Yorke | Kungaroo | Range Range Western | Murray

Speetes | Peninsula | Peuinsula | Island Area Area Aust. Mallee

E, camaldulensis + + = “fb + 4 +

hi, diverstfolic. = + - al = + +.

Ay tneritasedte + +- +- 4 -+- ni | +

4, conglobuta +4 a + i. Mia _

E. CRGEDS aL + +- ar ne x +

FB, rugosit + = + s + x +4

A, pileute + as {- = | + 4 <

EB. brachipenrlipe 4 = _ 4+ =, -_ oh

LE. leptophytla + + 4 4 4. +

El, apechyaeater + \ =, = _ ~ ae oe

B. alense + +4 + + =k + +

£. flocktoniae + 4 - = a 4 as

A. cahyeogorned| + } + 4 = ah + 4.

| 7

BE. gracilis + | + - 5 + o

EE. huberianc ~ = + = > ex +

E, leucoxylon. + = ee + + = +

E. caleicultrix + i + ~+ i He + = 4

fi, olovete + ' + + | | 4 = +

E, odorata var, nnyusti- + | e. — + + {?) = =

folic |

F. landslowneanu 4 4. = _ =; =

EY behrivant ! = +- + + + }

f \ |

EB. cladocalyse + = + + | — = =

22 20 i 15 13 14 13 15

: !

_., saurces of information for Tables 2 and 3: Baldwin and Crocker (1941), Black (1945-

52), Boomsma (1946), Burbridge (1947), Coaldrake (1951), Crocker, 1944), Jessup (1948),

Litchfield (1956), Northcote and ‘Tucker (1948), Rodger (1953), Specht (1951), Specht

and Perry (1948), and Wood (1930).

116 D. FL SMITH

fienres of Rodger (1953) for their general range. Thns a period of aridity when

rainfall fell, sav, 5 inches below the present level would eliminate all E. vbligua,

E. baxteri, and perhaps E. viminalis trom Lyre Peninsula and all but 2. eamel-

dulensis from Yorke Peninsula (and as there are no watercourse sites anyway

all six would probably be extinguished). £, oderata, which is generally recag-

nised as haying a slightly drier range than &. leneoxylon and E, cladocalyx, eould

survive on Yorke Peninsula,

TABLE 3

Climatic ranges of seni: creeds pis in Southey Aust redigr

| Mein Annual Reiifall

Mt. Lolts | Blinder Rewigsroo Kivee General | Wet Dias

Bpateies ) Range | tanige Ison =. Pentisula (lodeer) | (htoitcer)

— <= : . | ts =) ie ae. Vee ee a e2 = a

J, obtinuy | 85-45 | = a | — BO-50 f LOU

By ovina titling , p0-40 | — i 23 Bada fA LAO

I, hinwteré en -- Bt -— Le fH) TGQ)

LK. lenparylan £ AAA) 16 - 7 13-35 75-L3A

Be caaaldliutensis | 1KeBS Is — : la | ie> fails

Ke, ehiotaculigs 1s ' <2 OY Ta ) le2te FO-T1O

i |

| | Yorke — |

i i ! ‘ b Pearinsulu

| i | — ir

Max. ancillaries | 45° ' 305 i" 2R° 2 |

Mavs. no. wer daxsinrlvand | 150 how ta i 112 |

An Arid Period rainfall decline of the magnitude suggested by Downes

(195) would mean an average annual figure of 12-13 inches near Green

Patch, which now receives 23 inches. [f this was the moistest part of lowet

Eyre Peninsula, survival of Ee. cladocalyx, E. leucoxylon and even &. odorata

would huve been difficult, This suggests that the proposed rainfall decline in the

Arid Period is excessive, anc combined with evidence from Yorke Peninsula

(where E. odorata only has survived), a decline of 5-6 inches in the present

20-23 inches rainfall zone appears more likely,

Little is known of the methods or the range of dispersal of cucalypts, An

alternative explanation to that of Crocker and Wood — that the Eyre Peninsula

vegelation ts a relic of once widespread vegetation — is that all of these eucalypts

have been introduced by long distance dispersal from other centres. The

presence of 1. cludocalyx as a dominant without many of its usual under-storey

clements could be used as an argument for this, Its absence from Yorke

Peninsula. and the Mt. Lofty Runge, however, argues against this, Furthermore,

the E. cladocalyx on Eyre Peninsula is quite a different ecotype ocemring in a

different habitat (sce notes on individual species). In facet, the absence of

eucalypts from situations ig probably better evidence for the theary of Crocker

and Wood than their presence. A number of cases can be cited,

(i) The Distribution of Eucalypts on Offshore Islands.

From all information available it seems that the only cucalypts on offshore

islands are—

Boston Island: EB, conglobata, E. inerassata, E. eracilis,

Tavlors Island: Li. conglobata.

Thistle Island: EF. camaldulensis. LE. inerdssati, &. diversifolia.

PLANT ECOLOGY OF LOWFR EYRE PENINSULA, S.A, 7

If long distance dispersal was intensely operative one would cxpect a vreater

range of euealypts on these islands, and at least same on the other islands

which have none, all being relatively so clase to a mainkind rich in eucalypt

Species,

(ii) Vhe Distribution of E. camaldulensis.

This Free occurs only to the west of the watershed of the Koppio Lis,

despite the apparent suitability of several valley sites in the hills. It is sugwested

thal survival somewhers near Wanilla (possibly several centres) may lave

provided seeds which through water movement spread downstream to niuy

Ol the present sites, bit not over the divide.

(iii) The Absence of Cerlain Species near Sleaford.

A strip of Gayertine stretches from the west voust tu neur Port Lincoln, etfec-

tively separating the Tateritic soils of the Sleaford region from the main are.

Although no reliable rainfall data is available, it is obvious that it is at least

20 inches per wuinum, ie. quite a suitable habitat for EK, eludocalyx. Slight

valleys should be suitable for £. leucoxylon and E. odorata. Uf Jong distines

dispersal was operative to any extent these species should be present. On

the other hand, if the centre of survival was in the Koppio Hills and distriln-

Hen depends on migration, this belt of shallow soils on fienicetiae would prove

avery effective barrier to migration, giviwe the present distribution.

CLENERAL CONCLUSIONS AND DISCUSSION

The vegetation units of the area show w general similarity with wits having

the sume dominants elsewhere, A very detailed study of the Hundred of Stokes.

Which includes the north-western avd northern boundaries of the sugar gum

community, should prove worthwhile, Tt also coutains most of the other major

mits of vegetation, and has the advantage of having several large, uncleared

areas of serub, two al these being more than 5,000 acres each. Both appeared

to have escaped any major disturbance, sucly as firing, at least in recent years.

The Hundred of Kiana which studdles the margin of the travertine-capped

aeolianite of the western coast also has an interesting range of soils and un-

cleared vegetation, worthy of closer study, However, active clearing in the last

decide with extensive firing must have left a mark on much of this, The

Hundred of Flinders, which is a Mora and fauna reserve, has not been dealt

with in this paper. While the author has visited the western edge on several

oeousions, it was felt better to mit it than lo map it from aerial photos only.

tt apparently is largely a sandy and stony area like other coastal regions, but

there are several onteraps of Archacan rocks giving a range of soil types, and

some lateritie remnants. As climalie conditions are undoubtedly fairly uniform

throughout, a cetsiled study of this almost untouched area should also he of

great value.

ACKNOWLEDGMENTS

Grateful acknowledgment is made to the Titty Professor J. G. Wood, who

snegested this work and spent much time in stimulating discussion. Dr, R. Ty,

Specht has read the manuscript and made mony valuable comments,

In the field the Iate Mr. Worsely Johnston, Agricultnral Adviser at Port

Lincoln, was always a helpful critic and friend. My. Jobn Roc of Tumby Bay,

Messrs, Fo and W, Nosworthy of Lake Hamilton, and many other Hyre

Peninsula people assisted both in hospitality and discussion on land settlernent,

vegetation and soils.

11s D. F, SMITH

REFERENCES

Barpwry, J. G., aud Crocxen, R. 1.., 1947. The Soils and Vegetation of a Portion of Kan-

gatoo Island, South Australia, ‘I'rams. Roy, Soc. S. Aust, 65 (2), pp. 263-275,

Buack, J. M., 1945-52. “Flora of South Australia”, 2nd ed, Govt. Privter, Adelaide.

BuaKety, W, F,, 1955. A Key to the Bucalypts. Commonwealth Forestry and ‘Timber

Bureau, 2nd ed,

Boomsma, GC. D., 1946. The Vegetation of the Southern Flinders Ranges, South Australia

Trans. Roy. Soc. S$. Aust., 70 (2). pp. 259-276.

Boomsma, C. D., 1949. Nomenclature of Fucalypts with Specal Heference to Taxonomic

Problems jn South Australia, ‘Trans. Roy. Soc. S, Aust., 72 (2), pp. 221-227.

Buremer, N. C., 1947. Key to the South Australian Species of Eucalypts, Trans. Roy. Soe,

S. Aust, 7E (2), pp. 137-163.

Coatpnaxr, J. E., 1951. Ecology of Part of the Ninety Mile Plain, Sonth Australig, C.S.LR.0.

Aust. Bull, Na, 266,

Crocker, BR. L., 1944. Soil and Vegetution Helatiouships in the Lower South-East of

South Australia. Trans. Roy, Soc. S, Aust., 68 (1), pp. 144-171.

Crocker, B. L,, 19462. An Introduction to the Soils and Vegetation of Eyre Peninsula,

Sauth Australia. Trans. Roy, Soc, S$. Anst., 70 (2), pp. 63-107.

Cnockes, R, L., 1946b. Post-Migeette Climatic and Geologic History and its Significance ip

Relation to the Genesis of the Major Soil Types of South Australia. Coun, Sei. Tndustr.

Res, Aust, Bull. No. 193.

Crocker, BR. T., und Woon, J. G., 1947, Some Tlistorteal Influences on the Development of

the South Australian Vegetation Communities and their Bearings. on Coneepts and Classi-

fication in Eeology. Trans, Roy. See. 8. Aust., 71 (1), pp. 91-136.

Downes, R. G. 1954. Gyelle Salt as a Dominant Factor in the Genesis of Soils in South-

Bastémm Australia, Aust. J. Auvric. Res., 5, pp, 448-464.

Frenen, R. J., 1958. Soils of Eyre Peninsula, Dept, Agric. 8, Aust. Bnil. No. 457,

Jessuv, B, W., 1948, A Vegetation and Pasture Survey of Counties Eyre, Burra aml Kim-

berley, South Australia, ‘Trims. Boy, Soc. S. Aust, 72 (1), pp. 33-68.

Jouns, Tt, K,, 1961. Geological Survey of South Australia. Bulletin 37, $, Aust, Dept. Mines.

Lrenrmoo, W. H., 1956. Species Distribution aver Parts of the Coonalpyn Downs, South

Australia. Aust, J, Botany, 4, pp. 65-116.

Nowrucote, K. H.. and Tucxer, B. M., 1948. A Soil Suryey of the Huudred of Seddon and

Part of the Hundred of MacGilliyray, Kangaron Ishin, South Australia, Gown. Sei-

Industr. Res. Aust. Bull. No. 233.

Payor, L, D., 1955. A Hybrid Swarm between Kucalypiuy odorata and Eucalyptus leucoxylon,

Trans, Roy. Soc. S. Aust, 78 (1), pp. 92-96.

Roncxrn, G. J. 1953. ‘he Natural Qeeurrence af the Eucalypts, Commonwealth Forestry

and Timber Bureau. Leaflet No, 5.

Svan. D, F., 1960. M.Ag.Se, Thesis, University of Adelaide.

Sveout, R.L., 1051. A Reconnitissance Survey of the Soils and Vexetalion of the Hundreds

of Tatiara, Wirrega and Stirling of the County Buckinghn, South Australia. Trans.

Roy, Sac, 8. Aust., 74 (2), pp. 78-107.

Spectr, BR. 1, and Perry, RA. 1948. Plant Eeology of Portion of the Mount Lofty Ranges.

Trans. Roy, Soc, §. Aust, 72 (1), pp. 91-132.

Srecnr, RK, 1, 1963. Flora Conservation in South Australia, Pe. 1, Trims. Roy. Sue. 8.

Aust, 87, pp. 63-92,

Srepuens, C.G., 1943. A Soil Survey of Part of Hundred of Wunilla; County Flinders. Conn.

Sci. Industr, Res. Aust, Divisianal Report 22/1943.

Woon, J. G. 1930. An Analysis of the Vegetation of Kangaroo Island and the Adjucent

Peninsulus. Trans. Roy, Soo. S$, Aust. S¢ (1), p. 105,

Woob, J. G., 1960, ‘The Australim Enviromnent, third edition, C.SAR.O., pp, 67-b4.

D. F. Sarru

Fig. 1, Depauperate Eucalypins cladocalyx wou its north-western linsil

near Stokes.

Fig. 2. Large specimen ot FE, cladocalys wear Wanilla,

Trans. Roy, Sow. S.A) Vol. 87.

Db. F. Sain PLATE

Pie. lL. Ek. behriana near Curtiwilla Creek east of Curnmins,

Fiz, 2. E. camaldulensis at Koolidie Station homestead growing in traver-

tine limestone.

Fig. 3. Et. conglobata woodland on deeper soils of Boston Island near

Port Lincoln.

“Traus, Roy. Sow S.A.) Val. 87.

GEOPHYSICAL SURVEY OF THE OFFICER BASIN,

SOUTH AUSTRALIA

BY I. A. MUMME

Summary

A combined gravity and magnetic survey was conducted from Fisher (on the Transcontinental

Railway) across the Great Victoria Desert to Mount Davies, to investigate the possibility of a deep

sedimentary basin occurring between the Nullarbor Plain stable shelf and the Musgrave nucleus, as

suggested from the results of trial airborne magnetometer surveys conducted by the Bureau of

Mineral Resources in 1954. This gravity work shows that a significant "gravity low" coincides with

the assumed basin detected by the airborne magnetometer and also strongly suggests that such a

basin (which has been called the Officer Basin) actually exists.

GEOPHYSICAL SURVEY OF THE OFFICER BASIN,

SOUTHL AUSTRALIA

by I. A. Moxtme*

[Read & Novernber 1963]

SUMMARY

A combined gravity and magnetic survey was conducted from Fisher (on

the Transcontinental Railway) across the Great Victoria Desert to Mount

Davies, to investigate the pessibility of a deep sedimentary basin occurring

between the Nullurbor Plain stable shelf and the Musgrave miclens, as wnigduested

from the results of trial] airborne magnetometer surveys conrlucted by the

Bureau of Mineral Resources in 1954,

This gravity work shows that a significant “gravity low” coincides with

the assumed basin detected by the airborne magnetometer and also. strongly

suggests that such a basin (which has been ealled the Olfieer Basin) svtually

uxists, ;

INTRODUCTION

A series of gravity and magnetic observations were curried out at approxi-

anately two-mile intervals across the Officer Basiu ut the request of Exvil Pty.

Ltc., Sydney, to investigate the possibility of a sedimentary basin of considerable

depth occurring between the Nullarbor Basin stable shelf and the belt of ranges

situated along the N.T.-S,A, border comprising the Musgrave nuclens,

The possible existence of such a sedimentary basin wis brought to light by

an airborne reconnaissance magnetic survey conducted by the Bureau of Mineral

Resources during May, 1954. (J. H. Quilty and P. Il. Goodeve, 1958.) These

magnetic results indicate that the greatest thickness of possible oil-hearing

sediments in western South Australia are to be found in an area designated as

the Officer Basin which extends for approximately 100 miles south from the

known southern margin of the Musgrave nucleus.

PREVIOUS GEOPITYSICAL METHODS

The earliest geological and yeophiysical investigations in western South

Australia for possible oil-bearing sediments were confined to the Nullarbor

Plain area, and consequently the area occupied by the Great Victoria Desert

was completely neglected, for geologically it was considered to be of liftle

Interest

To 1954 the Commonwealth Bureau of Mineral Resources carried out 2

reconnaissance airborne magnetic survey over vertain areas of western South

Australia, aud adjoining areas in Western Australia, The arca surveyed extends

from Oodnadatta in the cast to Kalgoorlie in the west, and from the Northern

Temitory border in the north to the Great Australian Bight in the south.

The results of this airhornc magnetic survey indicated that the greatest

thickness of sediments in western Sonth Australia is to be found in the are

comprising the Great Victoria Desert. This sedimentary basin has been desig-

nated as the Officer Basin,

* Geophysivist, Department of Mines, Sonth Australia.

Trans. Roy. Sec. §, Aust. (1963), Vel, 87-

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GEOPHYSICAL SURVEY OF ‘TIE OFFICER BASIN, S.A. 12)

METHODS USED

(a) Geophysical Station Location

Along the belicopter traverse from Fisher ta the Gun Barrel road the geo-

phvsical stations occupied were located with the wid of scaled aerial photographs,

In the Great Vietoria Desert the stations vere located between dunes and

every fifth station was marked by a yellow flag,

Along the Gun Barrel road to Mt. Davies and along the road from Mr.

Davies to Oodnadatta, the statians cecupied were locitted from aeronautical

charts and fixed by speedumeter readinys.

The snrvey was carried out in four stages. The first stage was conducted

by hielcopter trom Fisher on the Transcontinental Railway (latitude 30°30")

for a distance of 180 miles along the 131° of longitude as far as the intersection

of that meridian and the Gun Barre! road ai a latitude of approximately 25°()'

(see plan 160-149),

Gravity, mitynetic and altitude meastirements were taken at intervals of

upproyimately two miles over this section of traverse, and SO stations were

oecupied,

The second stage of the survey was ronducted from station TL of the

hiclicopter traverse along a road Jeading towards Emu, and then up the Gun

Barrel road to the termination of the helicopter traverse at station 88. Gravity,

magnetic and cleyution determinations were mude, and 19 stations occupied in

this section of the survey.

The third stage of the survey was conducted from the end of the helicopter

» 3 any 4 a ad et

traverse (station $8), up the Gun Barrel road to Mount Davies. Thirty gravity

stutions were determined along this part of the traverse with an average distance

apart of 6:4 miles,

Magnetometer readings were conducted simultaneously with the gravity

reudings as far is station $6.21.

The last stage of the survey comprised a reconnaissunce gravity survey from

Monut Davies throngh Granite Downs to Oodnadutta (see plan L61-7).

Gravity observations were tuade on a number of astrofixes established by

L. Beadell (survevor) from the Department of Supply.

(b) Gravity Observations

The gravity observations were conducted with a World Wide gravimeter,

which hag a sensitivity factor of 0-11290 milligals per division. Absolute gravity

values were obtained by tying into gravity stations established by the Burean

of Mineral Resources.

The readings were reduced by applying the fallowing corrections:

(1) Drift correction,

(2) Elevation correction, and

(3) Latitude correction.

The gravity results were expressed as Bouguer Anomalies (in milligal units).

‘Vhe drift corrections were generally found ta be very small,

Elevations for the gravity stations werc obtained by microbarometer,

aneroid and altimeter measurements.

An elevation correction of 0-60 railligals per vertical foot was accepted

(which corresponds to a density of 2-67 grarames per «.c.),

122 I. A. MUMMT

The relative vertical magnetic intensity values were measured with a Hilger

Watt's vertical force magnetometer which had a sensilivity of 30-0 ywammas

per division.

To convert the magnetometer values into approximately absolute magnetic

intensity values a factor of 50,000 gammas must be added.

ig3"

| Mount Davi

MILES 5G

4 '

AUSTRALIA

GRAVITY INTERVAL If MALLIGALS

Inarparatiniy surveys by

| AMumme (8. A.Daptot Mines) and

Sanson andl Jvan De Linden (BMA)

WESTERN

BOUGUER ANOMALY PLAN

OFFICER BASIN REGION

S.A. Dept of Mines

(25°

Fig. 2. Bouguer ech plan of the Olfcer Basin and surroundings from results of surveys

condieted by $. Gunson, J. Van de Linden and I, A. Mummce.

CONCLUSIONS

The gravity work shows that a significant “gravity low” coincides with

the assumed basin detected hy the airborne magnetometer, and also strongly

suggests that such a basin (which has been called the Officer Basin) actually

oxists.

REFERENCES

Guxson, $., and Van pr Linnen, J.: Regional gravity traverses across the Eucla Basin.

Qurty, J. H., uid Goovrve, P. E.: Reconnaissance airborne magnetic survey of the Eucla

Basin, Southern Austrili:.

Trans. AMERICAN GuormysicAlL Union, March, 1960, Vol. 41, No. 1.

THE WOOLTANA VOLCANIC BELT, SOUTH AUSTRALIA*

BY RAYMOND CRAWFORD

Summary

Mapping of the Wooltana Volcanic Belt, Northern Flinders Ranges, South Australia, has shown that

2,000 ft. of Willouran trachytic lavas with minor andesites and rhyolites outcrop along the southern

margin of the Mount Painter complex and extend southward along the eastern boundary of the

ranges two miles beyond Wooltana H.S. They are overlain by Torrensian arenaceous and dolomitic

beds and those unconformably by Sturtian glacial beds. The area has been bisected by a steep

reverse fault (Paralana Fault) system, and associated splintering and wrench faulting is combined

with tight folding in the north and west. The northern part of the area is regionally metamorphosed.

Copper and asbestos mineralization is widespread. Gold, uranium and beryllium occur. Comparison

with other recorded Precambrian volcanics in South Australia, both in situ and diapirically

emplaced, suggests that the original area of extrusion exceeded 30,000 sq. miles. A general

comparison is made with volcanics similar in age and type elsewhere in Australia. A suggested

possible common origin with the Gawler Range Porphyry and Moonta Porphyry in South Australia

is discussed. The mineralization of the Adelaide System sediments is suggested to be exhalative-

sedimentary in type.

THE WOOLTANA VOLCANIC BELT, SOUTH AUSTRALIA*®

by RaymMonn Crawrorpt

[Read 11 April 1963]

SUMMARY

Mapping of the Wooltana Voleanic Belt, Northern Flinders Ranges, South

Australia, has shown that 2,000 ft. of Willouran trachytic layus with minor

andesites and rhyolites outcrop along the southern margin of the Mount Painter

complex and extend southward along the eastern boundary of the ranges twa

miles beyond Wooltana H.S. They are overlain Ly Torrensian arenaceous and

dulomitie beds and thase unconformahky by Sturtian glacial beds,

The area has been bisected hy a steep reverse fault (Paralina Fault)

system, and associated splintering and wrench faulting is combined with tight

folding in the north and west. The northern part of the area is regionally

metamorphosed.

Copper and asbestos mineralization is widespread. Gold, uraninm and

beryllium occur,

Comparison with other recorded Precambrian voleanics in South Australi:

both in site and diapirieally emplaced, suvzests that the original area of extru-

sion exeeeded 30.000 sq. miles, A general comparison is made with volcanics

similar in age und type elsewhere in Australia, A sugyested possible common

origin with the Gawler Range Porphyry and Moonta Porphyry in South Australia

ig discussed. The mineralization of the Adelaide Systciu sediments is suggested

to. be exhalative-sedimentary in type.

INTRODUCTION

Between July and October, 1957, the author mapped the eastern half of the

Wooltana one-inch Geological Survey Sheet, with particular emphasis on the

stratigraphy and structure of the volcanic rocks and the formations overlying

them. Mapping was done on South Australian Lands Department 60-chain

vertical air photographs, Petrographic examination of a large number of speci-

mens was carried out later in 1957 and a proportion of these selected by the

author have been described by H. W. Fander (see p. 155 this volume).

GEOGRAPHY

The area mapped lies in the north-eastern Vlinders Ranges, approximately

400 miles north of Adelaide, Wooltana HS. (139°27’E., 30°25’S,) les 25 miles

west of Lake Frome at the foot of the ranges, about 80 miles by road east of

Leigh Creek. The mapped area extends south from: Wooltana for six miles

along the scarp to Nepouie Creek, and north for 12 miles to Bast Painter Creek

(PL. 1, Figs. ] and 2). In the north, mapping has been extended westward about

five miles up the Arkaroola Creek to beyond its junction with the Wywyana, but

in the south reconnaissance mapping only has been practicable south of Mount

Warren Hastings.

” 4 Published with the vonsent of the Hon, the Minister of Mines for South Australia.

¢ Geological Survey of South Australia.

Trans, Roy, Soc. S, Aust. (1963), Vol, 87.

124

R. CRAWFORD

This whole area consists mainly of rugged hills with relief up to 2,500 fect

though predominantly between 500 ft. and 1,000 ft. At Wooltana a prominent

straight cragey scarp from 300 ff. to 700 ft. high (with Mt. Jacob) overlooks

the yast Lake Frome plains. This develops northward into a wider and higher

WOOLTANA, t

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Fig. 1,

Small-scale location map vf Australi «nd part of Australia.

THE WOORTANA VOLCANIC BELT, $.A. 125

zone of rugwed countey trenched by the great winding vorge vf the Arkaraala

Creek, West of it is the open Munyullina valley, widening southwards, itselt

limited westwards by another searp beyand which is monotonously rugged

country with Mt. Warren flastings as its highest poi. To the morth a most

confused tapovraphy reflects a complex structure and very broken country

extends west-ol the Barraranna goree of the Arkaroola (PL 2, Fig. 1) inte the

wrunite massif af Monut Painter (Pl 3, Fig, 2), The highest peuk wi the map

— Humanity Seat— lies on the east side of this massif; and further cast a large

embayment, south of Mast Painter gorge. forms a triangular urea of broken

gvonncd. ‘This is limited to the north-east by the Lady Buxton Creek on the

left bank of which are piedmont fangs in course of disseclion, Remnants of

these overlie the fuat of the Wooltan: scarp.

The Wooltana district, in common with the rest of the Flinders Kunyes, has

an avid climate with low and very variable ramfall, heaving very hot summers

and warm winters with cold nights. TRainfull is jutrequent and occasionally

torrential; though dissection is deep and close, no rnnning streams exist. Streams

are ephemeral. Waterholes are confined to the Arkaroola and Wywyann Creeks

and are alten dry.

The area covers approsimately filty square miles and contams two setlle-

ments, Wooltang ILS. and Arkaroole E.S,, with the total population of less

than 25, all supported by sheep vraziug, No nines are active. Motorable tracks

ave few but a road extends along the foot of the Wooltana scarp, and a reugh

track connects with Arkaroula throuwel the Munyallina Creek gap linking with 4

track coming north from Baleanootua.

PREVIOUS WORK

In comparison with the much more strongly mineralised grauite country

al Mount Painter to the north, dittle work has been done on the Wooltuna

ivnecns tocks; amd neurly alk that characteristicully hy Mawson, with one im-

portint paper by Woolnongh. A short account, larecly reeapituletory, is given

in Sprige’s unpublished report (1945) on the wartime reconnaissance survey OS

Mount Painter. Tf Woulnough’s sketch map of the Wooltana homestead unca

is oxelnded, no mapping uf any kind was done price t6 the author's except in the

extreme north where observations were recarded hy various Geological Survey

olficers working on the southern part of the Painter massif,

The first reference to voleanic rocks in the avea is in Mawsan's short note

ot 1912 in which he states that “intensive basic ignenus tacks are of common

oeemrrence in this (NE Seath easels} pre-Cambrian series. These are

partly coarse~ and partly fine-grained amphibulites and less altered uralitisecl

dolevites and basalts. The latter were observed to be amygdaloidal at an

outerop on the Arkavoola Creek...”

In his 1993 paper Mawson amplifies (his account, cspeeially mentioning

vesicular basalts just north of the gorge, and adding that “other parls of the

formation were breceiated dua manner which suggested a possible tuffaceous

charueter, The metamorphism which these rocks have yndergone obscures. their

features” (p. 390), A coarse-grained amphibolitic rock From the same area is

compared with the copper-bearing actinolite-rich rocks of Yoduamutana, More

space is given to vesicular Javas ~“amyedaloidal melaphyres” — from Paralany

station (uow a northern part of the Wooltana property) which he had not seen

in the ficld. These he considered to be recrystallised amygdaloidal basalts ancl

126 Rk. CRAWFORD

nuted. their close resemblance to chloritised basalts from the Blinman Suuth

mine described by Benson (1909).

The 1926b paper of Mawson is the most important, but suffers from lack

of w geological map; by chance the chosen line of section crossed what tg now

known to be the northern end of an outerop of post-valeanic pre-glacigene sedi-

ments, reduced at this point to a thin representative of an arkosie conglomerate.

Ifere it is peculiarly difficult to distinguish in the field either from one of the

many varieties of glacigene beds or from an igneous agglomerate, and was

classed by Mawson as the latter. dle therefore concluded that the voleanies

were “either conternpurancous with the glaciation or preceded it with no great

intervening time break” (p, 200), This was a reasonable inference from an

examination of the section alone but it is odd that in crossing from Wovltana

H.S, lo the eastern end of the section line Mawson failed to investigate the

prominent crags of the folded sediments immediately overlying the volcanics,

and the angular unconformity made by these sediments with the glacial

sequence, there most beautifully displaved, Eyen after further visits, one of

which ig mentioned in the only succeeding paper (Sturtian Tilite of Mount

Jacoh and Mount Warren Hastings, 1949) the very existence of these heds seems

to have been unrecognised, in spite of the fact that the area immedinutely north

of the homestead is the one place along the searp where they form the whale

of the lower part of the scarp and where no voleanies outerop.

W. G. Woolnough spent a short time at Wooltana in 1926 principally in

reconnaissance of the Lake Frome basin in search of salt on behalf of Brunner,

Mond & Co, He was evidently unaware of Mawson's discoveries and separately

described the Preeambrian weology with particular emphasis on the volcanics.

He, too, regarded them as directly under Sturtian glacials and drew a rough

geological sketch may of the area in the immediate vicinity of Waoltana HLS,

He noted the existence of bedded dolomites north-west and south-west of the

homestead, both of which he grouped with the volcanics, regarding the latter as

a merely local interruption of an essentially sedimentary series. and confined the

valeunies fo the area west of the homesteael,

GENERAL STRATIGRAPHY AND STRUCTURE

Introductory — Geological Environment

The Northern Flinders Ranges are defined here as those north of Blinman,

They forma wide zone of tightly folded Preoambrian and Cainbrian rucks, with

a (hingular outcrop, widest in the north, The essential structure is of eust-west

folds in the eentral zone, with north-west folds in the west and north-east folds

in the east, all characteristically asymmetrical. Much assveiated faulting, inelid-

tiv amajor thrusts, complicates the picture. It is further complicated by the

presence in the north-east of the outcrop of the oldest rocks, which form the

Mount Painter-Freeling TWeighits massif and its extension north The shape of

the outerop of this massif and the alignment of the houndaries between the

Archaean sedimentary and granitic bodies within it further demonstrate the

dominance of north-easterly trends; but clearly it has acted as a black mure

resistant to deformation than the Proterozoig and Cambrian beds wrapped

around it, and has had a strong iwiuence om the details of their deformation.

On the west and south of the massif upper Proterozoic rocks overlup it

uncanformably, West of Frecling Eleights in the Yudnarmutina area these are

predominantly sediments, though strongly inetamorphosed. Near Umberatana

THE WOOLTANA VOLCANIC BELT, S.A, 1277

cale-silicate rocks with possible volcanics appear. In the south the sequevve is

essentially volcanic with subsidiary sediments. It is this southern section which

is known as. the Wooltana Volcanic Belt,

Lower Stratigraphic Boundary of Wooltana Volcanic Belt

It is nol proposed here to discuss the Painter massif, the mapping of which

has recently been completed by the author's colleagues and in which he has

played uv negligible part. 1t has now been shown that everywhere on the

south side of the massif quartzfeldspar and quartz porphyries outerop nver

a belt usually 1-2 miles wide, They ave regarded as of Archaean age, aud

extend from the Arkaroul Creek above its junction with the Wywyana to the

Arkaroola Bore and Humanity Seat, the contact with the Wooltana rocks being

tectonic and marked by very strong development vf pegiuatites and a gigantic

quartz reef, The contact is broken by a major thrust—the Paralana fuult--

being stepped north on the east side and emerging from the ranges north of

ast Painter Gorge. ‘The eastern part of this stretch is an unconformity, aie the

contact can be traced through a small outcrop two miles east on the piedimant

slope, where it appears again to be non-tectonic.

South and cast of the Humanity Seat area no lower boundary can be traced

on the ground because of overlap by poorly exposed Mesozoic beds aud an

extensive further overlap of Cainozoic sediments. No relevant information is

obtainable from the wide network of bores on the plains, and it must be assumed

that the downfaulting to the east is on a major seule,

Upper Stratigraphic Boundary of Woultana Volcanic Belt

The accompanying yeological map shows that stratigraphically there are

marked differences in the thickness of the sequences on cither side uf the

Payalana fault, On thé east side the igneous rocks form a belt widening nurth-

ward und lying cast of, and stratigraphically below, a strong development of the

lower glacial sequence which is accepted as of Sturtian age. The map shows

also, however, that overlying the voleanies there is an arenaceous-carbonate

sequence present only near Wooltana in the sonth, but extending from the

area east of Lagle Crag northwards for several miles. Both at Wooltana and

at Woolnough Crag this is seen to be folded, and unconformably covered ly

the glacial sequence. Although very variable in facies along the strike, and

varying a good deal vertically, it is demonstrably arenaceous in its lower part,

with a characteristic dark arkosic grit and dolomitie ia its upper past.

The voleanies and. this arenaceous-carbunate sequence are therefore clearly

pite-Sturtian in age.

Towards the Paralana Fault intense folding, faulting and crushing make

mapping difficult, but the essential features remain, though the arenaceous par!

nf the sequence increases in thickness very greatly.

West uf the fault all the rocks are much more metamorphosed and thick-

nesses are again increased. The author's interpretation on the map is hased

on a recognition of the Sturtiin boundary, two miles up the Wywyana Creek

from the Arkaroola-Umberatana track; the areat arkose immediately north of

the track bein correlated with the arkosic grit of Wooltana and the equally

massive wide outerops of dalomites south uf the track with the overlying dolo-

mites. The phyllite sequence below the Arkaroola arkose is, therefore, a thick--

ened and metamorphosed equivalent of thin purple shales and quartzite tound

13s R. CRAWFORD

locally at Wooltuna and north of Groan Creek; und below it are dark greet

schistose rocks. with amygdaloidal lavas, much metamorphosed but undoutbedly

eguivalent to the Wuoltana igneous racks,

The more metamorphosed rocks of the Humanity Seat area are miueh Tess

readily identified by lithology and they are structurally almost completely sepiar-

ated Lrom those to the south, On the evidence of the unconformity orth af

Kast Painter Gorge they might he expected to be the equivaleut of the voleanic

sequence aud the overlying rocks. The uuthor, approaching them first from the

eust. saw little resemblance; but careful inupping from the south aeross the

Burraranna Gorge showed that the arenacenus sequence extends north into the

yradnally mylonitised rocks of Llumanity Seat itself, and a lithological hotmndary

in phyllitic beds has heen mapped to the east of the peak. Still lower in the

sequence is an actinolitic marhle almost certainly equivalent to one low in the

voleanic sequence. Tho anthor has siuce discovered that “possible ash beds”

were recorded within the lower less phyllitie sequence by Sullivan (according

ta Sprige, 1945),

The Use of the Term “Willouran”

Tn the past, the whole sequence below the glacial beds would have been

deseribed as Torrensian. In recent years the term Willouran has been used

for racks. in the Copley-Witchelina areca which are steativraphically helow the

Copley Quartzite. This is regarded as equivalent to the gredt arkose of the

Arkaroola HS. area. While such a division is easily applicable to that piu

of he Wooltuna Volcanic Belt lying west of the Paralima Fault it is less easily

applied ta the area do the east.

fn the West a considerable thickness of phyllites, apparently conformable

With the arkose, lie between it and the volcanics. The boundary between the

plivlites is in part faulted but in any ease metamorphism makes recognition

al its character difficult, ln the tightly folded central and northern area, east

of the fault, the phyllite sequence is little less thick and its base is again difficult

toa interpret, But sonth of the triangular area between the Lady Buxton Creek,

the Jault nmning sonth-west from the Lady Buatow Mine, and the Torrensian

guterap (ie, what is hereatter described as the “triangle of vuleanics”), and

in the whole of the scarp zone, the arkose is itself very much thinner, rather

loss persistent, wid is underlain by apparently eonformable thin quattzites or

shales which rest on an eroded surface of the yoleanies, "Chas the marked breuk

is here within whut is strietly a Willouran sequence,

{t would therefore biwe been easier to place all the tacks helaw the Sturtian

in one group, but to avuid confusion in relation lo published maps a division

into Willouren and Torrensian has been introduced and the break placed at the

bite of the arkose as elsewhere,

Willouran Series; Wooltana Volcanic Group

The Wooltana Volcanic Group in its “type” area, the Mount lacoh searp

zone, comptives hivas, taffs and agelomeratic tiffs with associated quartzites

and shales, The lavas are almost entirely sodic trachytes; sume andesite ocenrs,

Tutls are much less common than lavas and ure mostly found iu the south, where

u porphyritic sodie rhyolite bomb rock is locally common enough to produce

dguleput atic tiff. Tuff has beew recorded which is indurated, though net

welded.

THE WOOLTANA VOLCANIC BELT, S.A 124

Dykes are rare. Roeks having the appearance of dykes in outerop, but in

reality well post-voleanie and associated with later tectonic movements, being

either clasties Or-vein-rocks, ace very common,

Associtted sediments ave OF minor importance, Ib a sequence of approsi-

mately 400 ft. sonth of Wooltana HAS, green shales oceur, maximum thickness

30 tect, ator towards the tap of the sequence. One mile north of the HLS.

und again north ef Copper Mave Creek very characteristic rec, often current-

bedded, quartzites oeeur, These are lens-like in the south but in the north

cin he traced for long distances, They are everywhere less than 20 feet thick,

(Since the mup was drawn a bore at Wooltuna 1LS. has shown 200 ft, of red

quartzitio sandstone under the voleanies. }

Subdivision af the Wooltuna Voleanic Group is thought to be impracticable,

heeause of rapid horizontal and vertical variability,

In this scarp zane alteration of the reeks is very common and while the

type of alteration is usually clear, the pattern shows nothing but a consistent

regularity. The typical unaltered trachytes are Mason's “amygdaloidal melu-

phyres”— hard, dense, fine-grained, dark purple rocks with ‘salmon pink or

While ainygediales, or occasionally vesicular, They outcrap prominently, forming

searp edges and minor gorges. Rocks mineralogically Tittle different, but physie-

ally altered, occur as a purplish-grey or greenish-grey crumble on lower ground

between the outerops of unaltered but breeciated trachyte cemented by pink

and white quart, veins, which is common wear the major faults and in’ the

sduth-cast part of the “triunple™.

The small outerop of igneous rocks south of the Barraranna Gorge Mas

siniilax rock types, Chough near the fault they are mylonitized,

West of the Lady Buxton Pint lavas are confined to a small area near the

RBurraranna Gorge. Must rocks are green, fine-grained and tiffaceous, with

increasing scapolitization northwards. The proportion of shaly material is difi-

cult fo estimate. The sequence conhiins argilleceons limestones near the bases,

which become actinolitic marbles to the nerth, and a red quartzite higher in

the suecession which may be vorrehytuble with one of those of the scarp zone.

North of East Painter Gorge chlorite-magnetite schists ocenr,

West of the Paralana Fault metamorphism, tight folding, and faulting make

determination of original rack types very diffleult. Trne lavas are known to

occur only ina small area in Ue south-west, Green schists ave common, some

with quartz blebs possibly amygdaloidal in origin. The evidence suggests a

predammantly tuffaceous sequence between two actinolitic marbles whieh

coalesce westwards and open again west of the Arkaroola Water Mole revealing

another, smaller, outcrop of metamorphosed, mostly tuffacoous voleunics.

The Humanity Seat rocks are plivilites, with very minor volcanism.

Overlying Sediments of Willow'an and Tarrensin Series

In the scarp zone these rocks outerop in two distinct areas: a short sectinn

of the searp between Mawson Blill and Wooltana LES. snd a much longer

section extending from a point half a mile south east of Woolnough Crag north-

wards aroutid to the tighly folded Barraramia Gorge area,

The short outcrop thickens from nil at the south end of Mawson’'s. Bluff

to about 200. fl. at the maximum in the first creek north of the homestead, west

of which it is lost by folding under the Sturtian. The basal member is a red

quartzite (shaly at Wooltana) rising in the south through purple shales and

130 R, CRAWPFOKD

current bedded quartzitic sandstone to an arkosic conglomerate grit which in

(the north rests, discontormably on the basal quartzite, Above this very charae-

teristic grit (which is equated with the basal Torrensian to the west) bedded

dulumites outerep in the south; in the thickest section they have a light brown

mudstone at the base. There is much minor horizontal variation.

The sequence rests on an eroded surface of volcanics,

The longer outerop has essentially the same characteristics, with similar

horizontil variation within a general sequence beginning with quartzite passing

Wp into purple shales and arkosic grit. Above the arkosie grit and north of

Woolnough Crag a sequence of shales, fugey sandstoue, shales with minor dolo-

unites becomes regular, with the fagzey sandstone very thick in the north-east.

The overlying beds, purely dolomitic in the south, contain much shaly and silty

uitterial, Pre-Sturtian folding in the Woolnough Crag area results in Sturtian

resting anconformably on arkosic grit in the bed vf the Arkaroola Creck.

Accurate subdivision in the Barraranna Gorge avea is not easy, especially

north-east of the Corge where there is tight folding and much faulting. he

fagey member above the arkosic grit is apparently much thicker here and

dominates the antcrops.. In the tightly folded but unfaulted arca south-west

of the Gorge the sequence can be established, though very careful mapping was

necessary as squeezing ol incompetent members is common. Towards the nurth

churacteristic purplish ribbon-banded, ripple-marked quartzites become dermi-

nant below the thickened arkosie grit (and form the rucks in the sharp bend

af the Gorge itself) and can be followed across the Arkaroola immediately

vast of the Paralana Fault into the Thumanity Seat urea; slightly further north

in the immediate vicinity of the peak they are mylonitized aud no very ohviius

lithological correlation is possible.

West of the Paralana Fault the very couch thicker Willonran sequence of

inonotonous phyllites rises to a still stronger development of the Torrensian

urkosic grit well displayed in the gorge of Boulder Creck immediately cast of

Arkaroola H.S. The homestead itself stands on shales and westward the thicher

eyulvalent of the flaggy sandstone outcrops as another maassive scarp. Beyond

this is a very thick sequence of carbonate beds mapped in detail only along the

Wiayawyana.

Slurtinn Series

No detailed study of the Sturtian Series has been made, but its outerp

has necessarily been mapped and much information about the lawer and wpper

parts of the sequence was recorded.

The Series was examined tor the first time in this area by Mawson (14),

who gives’ detailed deseriptions along an east-west section near Mount Jaco,

Tt is necessary to add that inych lateral variation in lithology occurs, and that

Miuuwson’s belief iu the significance of the colours’ of tillites seems misplaced.

[In the scarp zone the Series varies a great deal in rock type. In the

southernmost area a basal boulder tillite is found, beautifully displayed in a

narrow gorge 2 quarter of a mile west af Merinjina Well (PL 1, Fig. 5). rising

into what is probably a luvioglacial conglomerate with sub-rounded pelsbles

und boulders almost entirely of quartzite, and aostly of xbout @ in. to 1 ft in

sive. The basal tillite is strongly purplish ar green duc to its content of volcanic

detritus.

THE WOOLTANA VOLCANIC RELT, S.A. 131

At Wooltana the same sequence is seed, but immediately to the north and

Fur several miles to beyond the Arkaroola Creek the lowest member is invari-

ably a ullite yery rich in rectangular blocks of dolomite, with other ervatic

inaterial quite subordinate or absent, This highly characteristic rock is the

material forming the massive feature named by the author Mawson Bluff, which

appears in the photograph in Mawson's 1926b paper. At this point the member

is thickest (100 ft.) and is a yellowish or buf tillite weathering dark brown.

In the creek on the north side of the Bluff it rises into a purple tillite containing

a much higher proportion of non-dolomitic material with the red bomb porphyry

very prominent. (in all the lower tillite containing volcanics, the hamb por-

phyry is predominant among voleanic erratics; most of the other voleanic types

have conwibuted principally to the matrix.) This member shows much Be

weathering and is less prominent in autcrep, Above it is grecner in colour

aud gives way te about 300 ft. of green and whilish shales, These are capped

hy the massive Huvioglacial couglomerate, forming great scars on the urest of

the range, The matrix of this is mostly quartz sand (vather than rock flour}

and the boulders nearly all fine-grained or inedium-grained quartzites, usinilly

pirple-stained with prominent current bedding. The rock is so indurated that

commonly the joint planes cut cleanly threngh the boulders,

North of Woolnongh Crag, which is formed of it. this lattes iinember oecuples.

newly the whole sequence; the outcrop is all high ground,

Iu general, the fuvieglacial conglomerate forms the inajor part of the

Sturtian outcrop, but the uppermost Sturtian along the custern side of the

Munyallina valley is again a definite tillite, with magnificently facetted boulders.

In the nerth itis intensely brecciated, and at the “tear-off’ north of Boulder

Creek, where the top and the bottom of the Series approach very closely, so

mich so that it is almost unrecognizable.

The Sturtian west of the Paralana DPault is confiued to the urea south of the

Arkaroola 11.8, Umberatana track, Tt has been examined in detail by the wuthor

only along a seetion up the Wywyana Creek, where there is uo sudden onset

at massive ghiaial beds but an introduetion of thin tillitic beds repeated and

wrudtiilly viving place to massive thivinglacialy which to the south are ore

developed and form the rugeed mass of whiell the highest point is uared

Mount Warren Tastings.

DVTAILS OF STRUCTURE

Faralana Fault: System

The major suuctural feature of the area mapped is the Paralana Fault.

This is a break which produwes an almost complete repetition of the scdimentury

and igneois fouuations, bisecting the area approximately mericdionalty,

It is a complex fuult, Beeause for much of its length it is a duplicates!

‘trike fault its existence was aot clearly estblished until the wartime yecon-

nuissance survey when air photographs became available for the first time. TPre-

viously, recognition was much more diffienlt hecause the area of majer tepn-

wraphie change on the west side of the Munyallina Valley. whieli was, of conese.

noted. both by Mawsen and Waolnongh, evincides with the eastern member of

the futlt, west of which is a warrow repetition of carbonate beds of similar

lithology ta some of those in the valley, this together with similarity of strike

and dip allaved suspicion, Neither Mawson nor Woolnough in 1026 —both

crossing westwards — so much as suspected the existence of au fault,

132 R. CRAWFORD

In Mawson’s L945 paper the existence af the fault is recagnised and. it is

shown on Sprigg’s reconnaissance map (1945) though the Wooltana Volcanic

Belt on that map is lett very; much in the air in relation to the rest of the area.

Mere we may regard the Paralana Fault System as beginning in the south

at ltalowie Gorge (see Fig. 2) on the Balcanvona I-mile G,S, sheet wliere a

double fracture throws the lower glacial muss on the west against upper

Sturtian on the left bank of the emerging creek, with repeated upper Sturian

between the two fault members. Tere they dip at a high angle. At this point

° SCALE

Ky MiLig 4 o 4 B MILES

i [|

GARDINER

Saale =MtfFreeling HS,

—

PARALANA

e@ Psrafena Hot Springs

"Old Paralana. HS. (Ruins) geist

aMulga Hut

LEGEND

EI.

EOP

ether

E/ 3 Sturtan lower gracias!

Ieatys 2 feguence

Arkaroola HS.

b 65D Torrensien arkose & equiwadat

Pl nces = beoliments

me Woolt | G2 Woattans Volrane Croup and

‘go fans comperdble “HiMouran

+ Granires porphyry & sediments

+ +] of Annter Conmpies

MT. MPIC AY yo Merinoen Series. Pm

—+— TTALOWIE ® Baleancona HS. Srervan Series __Ps

—}- GAP Jorrensien Series. Pt

Fouts —"

BALCANOONA —fr

Srachne —

3 2 Antichhe, a

2 Del AAT sWertaloonn H.5: & One Mile sheate— — _PARALANA

Fig, 2, Larger seale location soap of Northern Flinders Ranges.

THE WOOLTANA VOLCANIC GELT, S.\. 133

Hie mai amass of Startian Kaver ghcials on Une west side is tom off, re-appear-

ing in the area north-east of Arkaroola H.S.—a tear with an offset of 20 miles.

Culenlations based on cross seetions drawn through the centre of the Munyallina

valloy show that the throw-dowu ta the east is of the order of 25,000 £t. assuming

a dip al the faalt plane of 70") wad 29.500 Mr. at 80°.

The castern fault member is clearly exposed oa the uorth hunk of the

Baleanoour Creek four miles west of Baleanoona HLS, 250 viards north of the

track to Grindle’s Hut, immediately east of where the ereek Teaves the gorge

through Uv tiflite, [ere it is a low angle thrust, but u quarter of a mile further

west the westem member is a high angle reverse fault. throwing Lower Clacials

aginst upper Stirtian (on the cast), The western splinter is much stecper

and less clearly exposed,

North of Baleanoona Creck the northeasterly tending fault system is. offset

westwards hy north-south splinters whielt isolate Mlouwnt MeTuggart. From

there the easter member extends tor seven miles ina straight live, with the

western member about half a mile from it in the seuth but approaching more

closely northwards. This is the area where Mawson and Woolnough nucle

their veconnaissances, the “Cave Till dolomite” of Miwwson (1934) lying between

the faults and forming a very prominent east-facing scarp. To the east are

upper Startinn beds which iu the sonth include the upper vlacial sequence.

West of the double fault the lower glacials are very near in the south but the

unconformity between thent and the upper Torrensian swings away northwards

Jenving a wide auterop of the latter beds cast of Mount Wirren Hastinys.

A mile north of the paint where the Wooltana-Arkaroola track cuts throveh

the “Cave [ill dolomite” the tanltsare again splintered, with a direction chanve

fo north-north-cast ta north, Por several miles north the fault is a single high

angle stretch dinst (dip 70-80%) but inv the yiemity oF Boulder Creek and to

the south a narrow zone of upper Sturtian is duplicated, and at the north end

ol this duplication nassive quartz-iruon “blows” occur on the left bank of

Ronlder Creek,

From bere north the fault system as a whole is much more complex because

of intense splintering and wrench faulting on the eust side and to a smaller

extent ou the west side in the reverse dircetion, ‘The Paralina Fault proper,

however, remains exceedingly clear-cut extending across the Arkarovla Creek

upsheun from the Barraranna Gorge into the Tumanity Seat massif, passing

west of the peak, north of which it peters out into a complex system before

developing en echelon us the Paralana Fault of the “tvpe area” from north of

Must Painter Gorge to the Yudnamutana Gorge mouth snd Puralna Hot Springs.

At the point if crosses the Arkaroola, the break is so clean ent and lacking’ in

any local breeeiation (and this is true of much of its Teneth) that it is not

sirprising that Mavson failed to sec it (Mawson, 1923); here by relative north-

ward displacement of the eastern black against the Painter massif voleanies

of similar facies on each side of the fault approach very closely,

Splinter-Foulls and ‘Thrusts — Folds

Associated with the Paralana Fault System are several major splinter-faults

and thrusts, which ecxmnot be discussed without flie associated folds.

The most important of these faults extend asa Fan in a north-east quadrant

from the tightly folded area one mile worthi-east of Arkaroola ILS, Here, a

1H KR. CRAWFORD

tremendous compression on the cust side of the Paralana system has been

relieved by —

(a) overthrusting by the volcanics in the axial core, and the overlying

wwenavcous-dolamitico Group, on to the upper Sturtian;

(b) development of three tight anticlines with squeezing-out or severe

thinning of the less competent (largely ealearcous) beds in the arenmaceous-

carbonate Group;

— (e) (in the southern part of the Barruranna Gorge) minor over-thrusting

from the northavest, with petty wrench faults (all too small la shaw on the

THlp )5

(d) overtwming of the quartzites of the Burruranna Gorge at Het contact

with the volcanics at its northern end.

This is the situation in the “corner” of the structure, Beyond, the faulting

and folding extends well nerth of Kast Painter Gorge and affects the area around

the tipper reaches of Groan Creek. ‘The major thrust, (a) above, is probably

continued north-eastyard as the Lady Buxton Fault (unless that fault is en

echelon to it). On the west side of this the volcanic group is very tightly tolded

anticlinally with an overturned cast limb. On the east side the volcanics of the

“triangle” are for the most part folded more openly but in the south-west corner

of the “Uiangle” the arenaceous-carbonate group is lightly folded anticlinally,

with a curious shallow synelinal keel of quartzite between the principal anti-

cline and a subsidiary lying east of it, the two amalgamating north-eastward.

Stone wrench faults with very prominent slickensides showing horizontal mave-

ment are associated with this folding,

To the east and south of this comples system of folds and faults numerous

wreneh faults affect the remainder of the country mapped. These are nearly

all dextral on the west side of the lower glacial outcrop (some of these carry

through to the east side) and sinistral ou the east side: further south sinistral

faults become dominant. Many extend for several miles and have little throw,

but cumulative throw is considerable. They have caused narrow zones of intense

hreeeiation, Only the major faults have been mapped. Inmunerable minor

wrench faults exist and explain the ubiquitous brecciation in the volcanics. In

the glacials they Jead to much weathering-out of the rounded pebbles and

houlders of the fuvioglicial beds, where they are wot so indurated as ta farm

one solid mass, In the arenaceous-dolumitic group the effect is seen in the

shattering of the quartzites and in the dolomites shattering un an almost micta-

scopic seale is everywhere apparent.

As deseribed below in the Woolnough Crag-Vermiculite valley areca these

wrench falls are associited with what appear to be normal faults im turn

may be associated with the major downthrow limiting the ranges to the east.

Folding in this eastern area is much less common, the only important

exarnple being in the upper reaches of Groan Creck, where the dips in the

upper Torrensian arenaecous beds suggest a syneline plunging west, It is nut

cortain whether this is not partly to be explained by local thickening of the

grenaceous beds. The faulting on the north-east side of this area is also abnormal

in its north-westerly alignment, but this again may be connected with the faulting

linitiug the ranges, which clswhere is offset by north-westerly trending faults.

North of the Barraranna Gorge another major thrust, also duplicated,

develops from a fold in the upper Torrensian and extends purallel to the Lady

THE WOOLTANA VOLCANIC BELT. $.A. 135

Buxton Fanlt to Kast Painter Gorge entrance and beyond. This dips much Jess

steeply than the Paraluna Fault (and the Lady Buxton Fault); brecciation is

common and intense in the vicinity of East Painter Gorge. At the southem end

of this structure the phyllites of the Humanity Seat block are extremely tightly

folded and overturned

_ To the north the actinolitic marble of the Tumanity Scat block appeurs ta

be faulted against the higher beds; there is a marked difference of strike. Be-

yond, structures in the East Painter Gorge urea are very confused,

West of the Paralana Fault very strong faulting occurs along the southern

margin of the Painter Complex, principally along NE-SW lines. Tremendous

quarte blows exist, A crude en echelon pattern of wrench Caults affects the

Voleanies and sediments. Tight folding has taken place. Two major synclitics

in the upper Torrensian itre clearly established. (These fade southwards and

there is. no good evidence to date thern, even in part, as pre-Sturlian.) A little

uorth-east of the junction of the Arkaroola and the Wywyana folding is

extremely sharp and excellent boudinage is seen. Strong cleavage, clsewhere

not prominent, leads to weathering of the phyllites into angular blocks. The

zone between these twa syuclines is far from simply anticlinal, however, and

repeated examination on the ground and of air photographs has failed to

establish a satisfactory detailed structure, Variations in thickness of the voleaunics

wnd metamorphism make this difficult,

Further west, structures are simpler. They are finally cut by overlap of the

higher beds on to the Painter Complex.

A minor splinter cast of Arkaroola H.S. may partly account for the gald

miueralisation af the Golden Rule Mine (Lively’s Find),

Dyke-like Features

Two types of dyke-like features occur both of which are regarded as of

tectonic origin,

The first are brown-weathering lincar wall-like hodies which oceur in two

areas, the southern part of the scarp zone aud the eastern part of the area west

af the Lady Buxton Fault, both north and south of East Painter Creek, (In the

Jatter area some confusion may arise if it is not recounised that for about half

a mile south of the Lady Buston mine one has in fact heen used as a wall, with

debris of similar material piled on top or built on to the end as a dry stance wall

extension, ‘This is apparently an early shepherd's work.)

In the scarp zone these budies are 5-20 feet wide and extend continuously

(or with minor breaks) across the area in a north-north-easterly direction irre-

spective of the fonmations ontcropping. They reach 15 feet in height, usually

5-10 feet, and form strony landscape features, They are apparently vein bodies

of calcite, dolomite and quartz, rather ferruginous. No other mineralisation

had been noted,

Tn the Lady Buxton area the bodies are similar but north of East Painter

Creek they are folded.

In both areas the hodies are regarded as ves developed along wrench faults

vy associated fractures (including, perhaps, north of East Painter Creek, gaps

between tightly folded furmations).

136 h. CRAWFORD

The second type ot dyko-like bodies is confined to the sonthern end of {hie

scurp zone south of Wooltunt ILS. These are bodies with no differential relief,

istitlly only 3-10 feet wide, and dark or light grey in colour. Tn plices these

ent the tuffaceous shales, Le. they post-date at least the lavas of the south, They

wre Hol, however, volcanic, though they contain much altered yoleanic material,

Of hwo example collected (T.$. 5272 and TS, 5275) one is obviously a deeply

ulteved rack, largely caleite and chlorite; the other a strongly anylonitized ruck.

which Fander thinks might originally have been agglomerate or conglomerate.

At the time that these rocks were bein caumined, other rather similar rocks

were cQllected by Re -C. Worwite trom the Arrowie i-nl. G.S. sheet where he

has demonstrated diapirie squeeziug of Jower Torrensiwn material through

younger rocks along the eastern side of the ranges. Tb seoms possible thit

these wre related bodies, essentially tectonic.

LOGAL DE'VALLS Ol STRATIGRAPHY AND STRUCTURE

Wooltana ITS. Arca — Southern Lindt of Volcanies to Mawson Bluff

This is the awen of volcanics most easily seen, the Voleunie Group tere

forming a murow Jincar outerep no more tha at few yards wide in the extreme

suuth tad litle over half aomile in the north, The omlerop is broken immediately

novth of Woolkina ELS. by the overlying Vorrensian arenacceous-dolomitic group.

In this area. especially that part of it south of Wooltana ALS., faulting is

aomajor feature. In addition to mujor wrench fants, associated with which

are mumerons messive vein structures cutting the ontcrops with slrone: relief,

there isa thorough shattering. The area is also folded more intensely than any

ather part of the scarp vone. Much of the valeanie material is therefore highly

breeciated and is weathered more than elsewhere. Effects due to deuteric altera-

tion are not easily distinguished from alteration consequent upur tectonic

shattering and later weathering. Near the eastern edge of the outerop rock

types are commonly difficult to identity.

The scarp here is not more than 200 feet above plain level in the south, but

rises to about 700 feet in the north.

As the map shows, the urea is stueturally divided int) three parallel zones

by whut appear to be wrench faults. ach zone is anticlinal. with mild plonge

variation, so that several isolated outeraps of valeanic rocks oceur. The relation

slip of this folding and faulting which affects both the Yorrensian and the

Sturtian, to that immediately uorthavest of Wooltana, which affects only the

Torrensian, is not whsolutely clear: but there is uo doubt that the latter is

oldet: no effeet on the tillite northavest of Wooltana can be seen, but to the

south itis very definite. This folding and faulting with sorth-casterly ar north-

north-easterly trends is cotmected with the major flexing which limits the

Flinders Ranges as a whole,

The most characteristic rock type is exemplified by 'T.S. 3229, a amiweda-

loidal sadie trachyte (PL 1. Fig. 3). This is mueroseopically an unusually

stiking tock. a deuse fine-grained dark purplish-erey lava with amygdales

commonly filled with salmon-pink microcline and usually with white quartz.

Vesicular lavas of similar type occur, more especially in the south. Such

lava tops ave-common but not traceable for more than about 50-50 yards, they

dre repeated vertically uuny times, Beeause of such rapid variations and

vuriably intensive weathering and alteration counting of flows is impracticuble,

There is a contusion of numerous minor flaws,

THE WOOLTANA VOLCANIC BELT. §.4, 137

The fresh. unaltered trachyte commanly outerops adjacent to a crumble of

altered rock containing much sevondary material, VS. 3107. for example, is a

frachyte containing colowless to pale green amorphous material and calcite.

From field evidence there is no doubt that this is essentially the same rock a4

T.S. 3220, and a eradual chanze from the one to the other often uccurs over 2

distance Of 20 yards.

The third characteristic rock is the epidotised material, e.g. T.S. 3099. ‘This

aeeuts as sharply angiar fragments about 6 ins. long reserobling unweathered

talus, much Tess often as missive outerops, This is the host rock for tremolite

velo up to fins. wide. which ure commanly stained green with epidote and

ure sometimes crumpled.

The many breeetated areas commonly show a rock consisting of a traeliyte

simile to TS. 3229. but hroken tp into very irregular, sometimes crudely

rnnded maugsos comented together by quarts which is offen stained jand asso-

ciated with haematite. ‘Uhis material was ut first regarded ag an avelomerate

produced close to its sonree aud altered but once the intense and whiquitiuas

breceiation was recognised it was apprecivted that rauch of this type ol rack

is morely a recemented breeviated trachvle; some, however. is associated with

whut are almost certuinly small vents The frequency of aeeurrence ot this

tnaterial makes i diffiealt to he certain of the existence of pillow lavas, as the

only two phices where such pillows have Teen thought fo possibly exist ae in

areas of breeciation. Lmmediately behind Wooltana homestead strongly cleaved

red shales wppear to overlie the fives, bul they aqpear to he discoutornmalle.

The shales rise Chrough @& current-beddec sandstone and shales (40 feet) to

the very charactoriste arkosic conglomeratic grit,

To the south there is a generally low but very irregular area much cut by

thick veins of culvite, dolomite and quarly: further south the ground is higher

and ts cappecl by illite.

A clearer sequence is seen at Merinjina Well, one mile south of Wooltana

IS.) The Just wide curve of the creek before entering the plain below Merinjinu

Well windmill shows very clegantly the swinging onterop of the folded voleanics

under green tutfaccous shales. (‘These shales resemble part of the Sturtiwn

elacial sequence and there was at first some difficulty in distinguishing them

in the field.) The faulting of the voleanies against these is clearly sewn on

the left bank. Upstream for 800 feel is a fine succession of dark purplish-grew

laway, with veviexiia and amyedaloidal tops, all dippiny west at 30°-10°, and

showiryr the characteristic crumbly grey and yreen epidotic variants; these lavas

are of the order of 100-150 feet thick, At the repeated bowidary with the tulfa-

ceons shales a very fire seotion is seen on the lett bank, from which a suite

of specimens was obtained. A sketch of this is given (Pig. 3),

Vhe busal member is a fresh, liard, dark, grevish-green rock, non-vesicular,

vory constint in colour and texture, and with a smooth upper surface. ‘This is.

a micro-diorite (1.5, 5969) slightly courser-yrained and more basic than the

trachyles.

Tt is covered by a succession of interbedded tiffs and clayey sediments

and in the lowest tuff is a bomh of porphyritic sudic rhyolite, TS. 5265, with

characteristic glomeroporpliyritie chequer-albite,

This cryolite: occurs elsewhere. to the south and is very common as debris

at the extreme south af the volcanic outerop; it occurs rarely north of Wooltana

but it is widespread us av erratic in the Sturtian glactal beds.

138 R. CRAWFORD

The matrix around the bomb is a lapilli-tuff (T.S. 5266) but the immediately

overlying material is an argillaceous siltstone (T.S. 5270) succeeded by a tuff

(T.S. 5268) with similar constituents to T.S. 5266, Overlying these are tuffa-

ceous shales with pebbles of gritty sandstone, and a boulder of current-bedded

quartzitic sandstone,

In the extreme south a rock which appeared in the field to be a dyke

(T.S. 5272) cutting the volcanics immediately west of the major limiting fault

is strongly altered but most probably a volcanic which has been squeezed up

through tension cracks associated with the major faulting. A rock thought

to be a bomb is deseribed by Fander as a breceiated and mylonitized lapilli-

tuff or conglomerate (T,S. 5275). The only other volcanic characteristic of

this area is a very dense red jaspery-looking intensely hard ruck (T.S. 5271)

which is a tuff oceurrmg repeatedly among lavas and owing its colour to

/tt Green current-bedded silty shales

- “Pebble TES S267

Bins. Green tuffaceous shales Boulder of

curren? -

bedded

GUaPTZITIC

sav7ias7os7e

TS.5265 ox

AY;

B 7? OCH2 545, =

Tutt with bombs “6 origin 7.85720

7S. 8266

Dense /ava

3fK seen 78. 5263

Fig. 3. Sketch of vecurrence of bomb porphyry at Merinjina.

TIE WOOLTANA VOLCANIC BELT, S.A. 134

abundant haematite. ‘This rock has not been scen in the northern part vf

the Belt, but much of the tufluceous material there is comparable though less

haematitic,

Between Wooltana H.S. und Mawson Bluff is the area first deseribsr by

Mawson (1926b), On the low ground north of the hills occupied by the upper

Torrensian the voleanies outcrop poorly under piedmont debris. The yeddish

sundstones and chocolate shales described by Maavson as below the main igneous

formation have not been seep. Eustwuards the boundary of the volcanics and the

averlapping ?Cretaceous conglomeratic gravels is indefinite. The first major

creek to the north-west offers a poor section in the voleanies (though a fine

une inthe higher beds), Further north the outcrop of the volcanics widens at

the expense of the upper Torrensian and the three characteristic rock types

mentioned earlier are well scen, in their equally characteristic irregular distri-

bution. The strike is generally north-westerly with a dip south-west of 20-25%,

in sympathy with the synelinal folding of the upper Torrensian. In this arca

interbedded sediments are rare, except in the extreme north where quartzite

lenses appear,

Meauwon Bluff to Capper Mine Creek

This area has been examined in most detail in the south, where the strati-

graphy is appurently mast complex. A typieal section is seen in the creek

running, from the amphitheatre of Mount [acob down on the north sid of

Mawson Bluff.

The southern part is apparently more disturbed than the rest and has mneh

more interbedded sediments. mainly red shales, purplish-grey conglomeratic

shaly sandstones and minor quartzitic sandstone. As in the south, repeated lava

flows are common. The relation between the Sturtian and the voleanics is here

apparently only disconformable becanse of similarity of strike and dip. fmme-

diately north a tight syncline forms a steep Inll, volcanics in the hill heimg

faulted against sediments in the creek to the north.

Jn Red Bank Creek a hard dense unusually reddish rock was noticed ncue

the Sturtian boundary. It is an indurated tulf (T.S. 3213),

The only other rock exumined which resembles this is T.S. 3143 from ihe

isuluted outcrop of valeanies adjacent to the Paralana Fault between the Bar-

rutsuita Gorge and Arkataola HLS., a resemblance net obyious in the field, as the

rucks in the latter areca are much breeeiated and squeezed. In the author's

vpinion the two types are different, T.$, 8213 being probably indurated by super-

meumbent strata or baked by overlying lavas, and T.S. 3143 being a tectonically

jiwetamorphosed volcanic.

The area between Red Bank Creek antl Woodnamoka Creek presents no

uiusual features, having a little sedimentary material and nurneraus. typical

flaws. Jt has two prominent hills, outerups of massive dense red-brown rock

which in the field resembles T.S, 5213, but which has not been examined miero-

scopreally.

At Woodnamoka Well typical vesicular und amygdaloidal lavas are beauti-

fully exposed. Epidotized rock is common here, c.g, T.S, 3228 (Pl. 1, Fig. 4).

Above Woodnamoka Well similar rocks are repeated across all the outcrap.

North [rom Woodnamoka Well to Copper Mine Creek there is a greater

regularity of outerop, but insufficient me could be devoted to the area tu

Li R. CRAWFORD

determine whether this is due (as farther north) to an increased proportion ot

intercalated sediments or to some other reason, eg. lineur fissure eruptions ws

against the confused and apparently more explosive conditions of the Woolhana

HWS. area, It is probable that both causes cuinbined to give this effect.

Vermiculite Valley and Croan Creck Arce

This is a huge area of westerly-dipping lavas with minor sediments, with

clourly defined faults — either normal or reversed, but not wrench Faults —

markedly affecting the lamdscape aud prodneing the fault-angle depression of

Vermicolite Valley. it has been subjected ta two perinds of folding. The

first period af folding is illustrated hy the existence of a tiny outcrop of volcanics

occmring West of the upper Torrensian outerop, und is uneonformable iwuder

the Sturtian. The whole of the north-cast is uently arched alone the north-

south axis as is revealed by the present disposition of the Mesuzoie (Cretaeeuus )

cover, "This latter folding is insullictent to alter the general westerly dip of the

volcanics.

Rocks typical of the Wooltata area oecur, The typical amygdaloidal lava

is most easily seen where the old Pavalana mail track crosses the Arkarocla,

Ou the south side up the ereek for a quarter of a mile is a heautifidly exposed

succession of lavas many of which are umyydaloidal sadic trachytes (#8. 'T.S,

3220, PI. 5), and the recemented breceiated variety is very COMMON a quarter

of a mile to the south-west (ed. T.S, 300-4),

On the west of this lava belt of wninor rmgged hills a continuous entero

of uw thin durk red very detse recrystallized quartvitie saudstone Hmits the

eastern edge of Vermiculite Valley, Two specimens uf this have been examined

(T.S. 5277 und TS, 5278), are ubnest identical and resemble red quartzites

from the “triangle” and the area west of the Lady Buxton Fault, Though it

would be unwise to assume that they are all necessarily svnchronous. they

ovable the stratigraphy and structure ta be disentangled in the three separate

areas, iA Which the outerap is continous or alinust so.

Vermiculite Villey itself is a generally flat-bottomed valley strewn with

debris of piedment material (which caps some of the yolcanie Wills) and much

weathered volcanic rock, It is an enigma. being dike mo other part of the

voleanic outerop execpt the eastern part of the trianvle, where, similarly. much

weathered yoleanie rock exists, One is tenypted to regard it as perhaps ut ove

lime very temporarily «lake, since drained by a right bank tributary of the

Arkavoola about hulf a mile above the Varalana mail track crossing. A high-

level Juke Frome (and there is much wnpublished evidenee of such a former

high-level) would fill the valley and have marked effects on the rock weathering,

A eurious depression. reminiscent of wa old mine shaft ynd dump area so

completely washed hy rain as to he almost unrecognizable, occurs in the centre

uf the valley about L00 yards east of a sizeable fault searp. The material in the

“dumps” is a crumbly crust of wrey-green weathered yolcunie rock and was

Sampled as a possibly aetivatable clay, Mrs. N, Chebotarev examined this

and found it ta be mostly aggregated vermiculite with much secondary iron

mineral. The rock at the foot of the fault scarp to the west (TVS. 5276) was

fond to be a completely altered fine-grained volcanic.

North of the Arkaroola, Groan Creck is a major lett bank Uibutarv, cust

mf which mast of the volcitnie outcrop is strewn with younger debris: in the

savith the volcanics are better exposed but very much lateritized on the crests.

THE WOOLTANA VOLCANIC BELT, S.A. 141

This is an interesting area not examined in detail, T.S. 3225 from the central

part of a fuw towards the north end of Groan Creek snuth-east of its exit from

the upper Torrensian is a slowly-cuoled trachyte, This rock type is very

cammen in the area, together with typical amygdaloidal trachytes.

“Triangle of Voleanies”

A relatively small but highly confused area of volcanics exists as a triamemilar

area between the Lady Buxton Fault, the upper Torrensian, and the Lady

Buxton Creek, This contains all types of voleanies previously described, but

tight folding in the southavest, and deep weathering towards Lady Buaton

Creek, made identification cccusionally difficull, The south-eastern part is

intensely brecciated and contains same isolated knobbly hills which are probably

venigs,

A typical lava (7,8. 3224) from the southern margin is a sodic trachyte;

T.S. 3169 from the eastern edge is similar bnt coarser grained.

A rock from one of the knobs considered to be possible venis is T.S. 3194,

another tuchyte.

South-westwards these rocks give way to ereen fine-grained rovks with

quartz blebs suggestive of elongated amygdules. Ilalf a mile south-yest of the

Ludy Buxton mine an altered andesite wats collected (T.S. 3232).

The northern and north-western part of the triangle has been shawn tu be

anticlinal by following the outerop of a quartzite comparable with those de-

scribed ahove.

The proportion of tuffaccous material increases iu the north-west, so_ that

the succession tends to resemble that of the arca west of the Lady Buxtou Fault.

Arca South of Barratanna Gorge

A small outcrop of volcanic racks oecurs immediately east of the Paralani

Fault on the west side of the track running north frora Boulder Bore. This. is

an anticlinal core of rocks brought up by plunge variation. The volcanics are

typical Wooltana-type amygdaloidal trachyvies with mimor tufts but adjacent

to the fanlt they have been mylonitized.,

Arca West of Lady Buxton Fault ane Lust of Mimanily Seat Thrust

A ruveed acca between the “triangle” and the Himnanity Seat mass extends

from Barriranna Gorge to East Painter Gorge. North of the entrance to Mast

Painter Gorve a smaller avea of similar rocks exists. This is the northernmost

recorded Guterop of the Wooltana Voleanie Group,

These rocks (a) are generally much siove (nflaceons than those to the cast

and south; (b) contain more persistently hedded sediments — dolomites, actino-

litic limestones; (¢) are tightly oyerfolded in an anticline along a narrow zone

parallel to the fault; and (d) show inereasing metamorphism from south to

north,

‘True lavas ae seen only in the extreme south next to the overturned sand-

stones through which the Barraranna Gorge is cut. Most of the area shows

hedding on the air photographs.

‘Three rocks from the south centre of the area are TS. 3191, a strongly

altered hasie rock, T.S. 3192, probably an altered trachyte and T.5, 3144 (from

142 R. CRAWFORD

the foot of the thrust in the south-vest}) an extensively altered fine-grained

ignedus rock,

The rocks of the uorthern part of the area arc very much scapolitized and

the question of the existence of spilites was considered, An example is TS.

3184, a thoroughly seapolitized rock. No detailed study has been made of these

rocks but they are at present regarded us comparuble with those to the south,

wtered mainly by regional metamorphism with accompanying metasomatism.

Another related rock from about 200 vards northayest of the Lady Buxton

Copper Mine was deseribed in the field us a “seapolilized intrusive or ?spilite™

(TS. 3088). Petrographically this resembles the albite-tremolite rock from

Groan Creek (TS. 3225}.

Narth of East Painter Creek chlorite-tnagnetite schists are characteristio

(T.S. 3149). In the extreme uorth amphibolitic material appears which is not

certainly part of the Group, being possibly part of the Painter Complex,

Arca West of Paralana Fault

This area, much less readily accessible, has heen studied im Fess detail thay

the rest. Tt is intensely folded. True amygdaloidal lavas have been observed

in the south-west. The rest of the osterop would best be described as green

schistose ¢alc-silicates, but green quurtz-blebhed dense rocks oveur in the north

which are regarded ay metamorphosed atnyydaloidal lavas, eg. T.S, 3214,

Still further west, bevond the Arkaroola Water Hole (ie. 1-18 miles west

at the Wywyana Creek ) similarly metamorphosed rocks occur, and one specimen

from an Guterop surrounded by actinolitie limestone belongs to the amphibolitic

facies (T.S, GL74), a very characteristic pink and green feldspar-tremolite rock.

These rocks — which are Mawson’s (1948) Arkarooka Serics—are cut off

westwards by the unconformity of higher horizon rocks on the Painter Compley

but aré thought to be the equivalent of amphibolites near North Well, east of

Umberatana HS. which ure at a comparable stratigraphic horizon.

Hrnmenity Seat Area

The Humanity Seat area is quite different from the others described, being

much higher, more rugged, and essentially an area of phyllites. However, there

iy little dowht that these phyllites are sttatigraphically equivalent ta the Voleanic

Group on mapping evidence. None of the volcanics noted by Sullivan have

been seen by the author, as Sprigg’s report oa the area, in which this oveurrence

ig quoted, was not seen until field work was completed. The existence of an

actinulitic limestone east of the phyllites suggests equivalence with thase highly

folded in the arca west of the Lady Buxton Fault and similar limestones west

of the Paralana Fault: and the uppermost very mylouitic rocks adjacent to the

Pauralanid Fault can be followed along strike southwards into upper ‘Porrensian

beds.

MINERALIZATION

Mineralization is widespread in the voleanies and along structures, The

observed minerals of economle interest are those of copper, gold, uranium and

beryllium, and asbestos (tremulite). Magnetite occury in the north and the

volcanics are everywhere yery rich in haematite, The gold is not certainly

ussuciated with the volcanics, but is of much interest, Cave guano and ammu-

niacal cave deposits ace known in the carbonate rocks.

THE WOOLTANA VOLOANIC BELT, S.A. 13

Copper

Minor malachite and azurile showinys ~rve numerous, mostly along or near

faults, The largest occurrence is at the Lady Buxton mine where mineralization

Is associated with strong overfolding and thrust and wrencli faulting. Magnetite

occurs here also, and a quarter of a mile further north.

Woodlamulka mine on Copper Mine Creek bas less obvious mineralization.

Six shafts were sunk along a shear which is probably related to the wrench

faulting described above. The Oraldina, Great Boulder (Creat Boulder and

Welcome) and Wheal Tlancock Mines were all in the vicinity of Boulder Bore,

near the Paralana fault and Golden Rule gold mine (qv. i. Several other minor

digvings and more showings exist cast of Groan Creck. in the high ground west

of Vermiculite Valley, in the triangle, and in the “Llear-off" area nortli and

nuith-cast of Boulder Bore. The old shafts two miles north-cast of Boulder

Bore are at the junction of the Sturtian glacials with the overlying slates, here

a fault, These may be the old Kingsmill Mine. Other minor shows are seen

in the Barraranna Gorge (suuthern part) where they ave clearly related to

faulting, though Woodmansee aud Jolmson (1956) suggested that some may

he derived from leached volcanics, The sume authors recorded bornite in

vesicles near the Arkaroola Bore.

The O'Donoghne’s Castle mine was on the Paralana fault about six miles

south-east of Arkaroola HS. The Nepowie mine (never developed) was

adjacent to Nepome Peak, probably on a wrench fault.

Asbestos

Tremolite has been dug for at two sites near Wooltana H.S. and most oveur-

rences of tremolite in the scarp zone have obviously been prospected, ‘They

are clearly related to faulting, often cecurring in fault planes. No importint

deposits have been seen, though if the occurrences. were near to Adelaide some

might prove workable.

Gold

In 1949 three prospectors discovered gald about three-quarters. of a mile

vast of Arkaroola HS. (Lively’s Find; Golden Rule Mine). This is sited almost

exvelly on the Paralana Fault. 158+85 fine ounces was produced from 77-1

tons of ore dug to 1952, The last working took place in 1954.

The 20 ft. shaft has not been descended by the present writer, and the

statement by L, L. Mansheld (Mining Engineer) that the material excavated

appears to be a decomposed and fanited dyke has not been verified; ouly shales

haying been seen. Petrological examination of this material by A. W. G.

Whittle in 1948 and 1949 indicated that the material might be of primary

origin, and a report by F. L. Stillwell in 1949 on a specimen described it as

a fine-grained syenite-aplite. This suggests that it is cither an altered thin

retunant of veleanie material preserved along the Pardlana fault plane or similar

voleanie miuterial as debris in a conglomerate of upper Torrensiau ave: or

mylonitic volcanic material squeezed up locally along the fault plane. Voleanies

outcrop a quarter mile north,

Cramton

Woodmunsee and Jolinsan (1956) refer to scattered evidences of uirtinium

mineralization m small amounts in the area west of Paralana Fault, in the

actinolitic marbles, associated with copper mineralization, They regarded it as

unimportant.

ltd Rh, CRAWFORD

Berylliun

A speciien from the dumps of the Lady Buxton Mine has been described

by IL W. Pander as conttining massive magnetite with veinlets of malachite

wud purtly altered crystals of phenacite.

Woolfana Cave

References wre often made to the Wooltana Caye. This is the Ammonia

Cave of Miowsou (1934, map, p. 188) and Ammemia Mine of Woolnough (1926).

The cave is i mussive doloanitic limestone immediately west of the Paraluia

Fuult (cast member), near the Woultana-Arkarogla track and when visited by

Woolnaugh in 1926 contained quantities of liquid wallaby dung. Near the

entauce a greal heap of bat wuuno was seen, in while the remains of a large

extinct bat-eating bat were discovered, demonstrated to the Royal Society of

South Australia by Wood Jones in 1925. The floor of the cave was covered

with ammoniacal material later dug tor manure, and Jast worked in 1933.

COMPARISONS WITH GTOER AREAS

Areas on Margin of Painter Complex

As pointed Gué above (General Stratizraply and Structure), upper Pro-

terozoie rocks overlap uncontormably the Archaean rocks of the Painter Con

plex on the west side as well as on the sonth,

Near Umberatana, rocks ocenr bvo miles north-east of North Well (which

is on the Arkaroola track six miles east of Umberatana) and have been mapped

by Thatcher as citle-silicate rocks. Some of these were seen by the author and

uppewred very similar to the westernmost Wooltana VYoleanic Group reeks. They

are ina comparable stratigraphic position, helow the thick urkase. No detailed

exumimition of the rocks has vet been made,

At Yuenamntana, eight miles east-north-east oF Umberatana, copper minera-

lization has lung heen known to be associated with basie rocks. Mawson (1923)

described altered basic intrusives “post-dating the grent quartzite” which at that

time he eyaated (with some hesitation) with that of the Bolla-Bollauw (Bar-

raranna) Gorge. He noted much actinalite and tremolite, Recent mapping

hy Campana, Coats, Horwitz and Thatcher places these rocks in the Willouran;

bul they ate, of course, a horizon equivalent to that of the Wooltana volcanics.

One is deseribed by Mawson as a diubase, A specimen colleetetl by BR. P.

Coats during mapping has been described by A. J. Marlow as aimphibolitic

miarble, and another from Wyo miles cast as 2 pyroxene marble.

A little further round the periphery of the complex, altered basic intrusives

were recorded in the vicinity of the Daly (Minvson, Daley) mine, four miles

eust-north-cast of Yudnamnutana. Mawson described some as “slightly vesicular’,

and intruded into “slaty and calearcous beds”, adding that the intruded rocks

“include a remarkable development ot aclinolite rock and spotted slates in

which tremolite is seen to be forming at scatterud centres. crystallizing in radial

fibrous forms”. This association of rocks is almost identical with that on the

oppasite side of the massif at the entrance to Kast Painter Gorge. Again, recent

Geological Survey mapping places these rocks in the Willouran. Two miles

suet of the Daly Mine a seapolitized hasic rock was recorded at the Shamrock

Mine.

THE WOOLTANA VOLCANIC BELT, S.A. 145

Arrowie One-Mile Sheet

In late 1959 mapping by R. Horwitz on the Arrowie one-mile sheet 40 miles

south of Wooltana revealed basiv rock iu breceias apparently squeezed up along

the margimal fractures of the ranges near Tea Tree ontstation and St George's

Bluff, Three specimens collected by Horwitz were described by Funder as

a dolerite, a uralitized dolerite and a sheared uralitized gabbro and it seems

likely that these are oF Willouran age. They are fragments diapirically em-

placed in Marinoan and Cambrian rocks. Other similar associations haye heen

mapped in the area to the west.

Bliranan Dome and Other Dinpirie Structures in the Central Flinders Ranges

The Binman Dome is a prominent structural feature of the Central Finders

Ranges. Howchin (1907) recorded basic rocks in “voleanic dykes and necks”

near Blinmai, where a rich copper deposit was found in 1862 and worked till

L915. Specimens were described by Benson (1909). Howehin (1922) gave

turther details and ulsy referred to hasie intrusions at Big Hill, Wirrealpa, 15

miles east. Dickinson (L944, 1953) deseribed the mine: and accepted Howclin’s

“intrusions, suggesting thut they were, however, separated from the upper

Proterozoic and Cambrian by an uneconfarmity and that they predated the

diastrophism which produced the Dome. Howard (1951) studied the distrlot

and revarded the structure as an “early form of ring-dyking” and thought the

husic rocks were intrusions following a late slage of The Cambrian to post-

Cambrian folding and faulting, He formd rio uneeniormity. Te did sumuest

that Benson's “melaphyres” predated the dolerites and were interbedded with)

shal and sandstone,

Webh (1960, 1961) recognised diapirie structures in the Flinders Ranges

of which the Blinman Dome is one of the largest, Most of the rocks in the

diapiric centre are of Willouran type and inclacde lavas. Subsequent detailed

mapping by Coats and Webb shows that many of these Invas though aften yery

similar to Woultana type lavas are rather more. basic,

Comparable dinpiric strretures occur 15 miles east of Blinman near Wie-

revlpa ELS. 20 niles south near Orapariuna H.S,, 40 miles south near Arkaba

Hs, and 55 miles south near Worumba HS. Of these, that at Oraparinna

includes large outcrops of amygdalvidal trachiyte identical with some Wooltana

trachytes. The Worumba area was deseribed by Spry (1951) who recognised

uralitized and saussuritized dolerites and basults. The present author (1930)

noted diorite in crushed dolomitic limestones near Arkaba.

Leigh-Creek-Angepena Area

Benson (1909) refers ty a dyke at the Vietory mince, 10 miles east of Leigh

Creek, Northern Plinders Ranges, and describes a specimen as amy gdaloidal

mélaphyre, ‘This was probably from the “dolerite plugs” mapped by Parkin,

Reyner, Pitman and Johns (1953) on the Serle one-mile sheet as intruding the

Shirtian south-east of the Victory mine. Similar dolerite plugs are mapped on

the Angepena sheet to the south, by Sprige and Wilson (1953) at Camp Hill

Sprinus —almost on a fault—and im a great “crush zone”, possibly diapiric,

north of Mucatoona Hill; and cast and north of Leigh Creek and at a si on

the North-West Fault near Termination Hill by Parkin and King (1952) on the

Mirtle Sheet.

146 Kh, CRAWFORD

Willonran Ranges-Witchelina HS, Area

Howehin (1924) deseribed Sturt tillite in the Willouran Ranges west and

south-west of Heryott Springs (now Marree). Masson (1927) gave further

details of the geology, Howchin noted no igueous rocks in situ, but saw many

varieties us -erraties in the tillite.

Mawson (p. 387) mentioned that a microscope slide of a conglomerate of

a “peculiar type” at Breaden's Hill showed a fragment of a much-altered ophitic

basic igneous rock, suggesting that it may have originated in a dyke located

amongst the strata hall a mile to the west. He described the beds ta the west

and named them the Willouran Series, noting a cale-silicate rock between

Breaden’s Fall and Hogan's Well and ua large ophitic dolerite sill, wralitized and

epidotized, “extending for a great distance tothe north-northavest” (fram

near Breaden’s Hill}. This, he said, “it quite like some of the basie igneous

types of Wooltana and Blinman”, He noted also vanadium mineralization (as

well us capper ),

The published Goolugical Survey sheets do not cover this arca but a speci

men collected by R. K. Johns from Tour miles east of West Mount, Witehelina

onesnile sheet (and 25 miles south-vvest of Marree) is an extensively altered

medimn-grained volcanic similar to thase of Wooltunat, Specimens from Wil-

lanran rocks near Cullana ELS. mapped by B. P. Webb include vesicular dacites

ane) utierodinrites.

Port Augusta-Lron Knob-Whyalla Arce

Forty miles uarth of Port Augusta, Brunnschweiler (1956) recorded amygda-

loidal lavas in Willonvan rocks at Depot Creek, Southern Winders Ranges. These

ure identicul with the bypical Wooltuna trachytes.

Early in 1960 B. P. Webb, visiting the Whyalla area with R. Whitehead,

veologist of Broken Hill Proprietary Ltd... collected similar lavas from a sequence

interbedded with sediments unconformably overlying Archacon at Doulas

Point, on the coast of Spencer Gulf south-west of Port Augusta.

In mapping the Middlehack Ranges. Miles (1955) recorded “younger

dolerite dykes and possible sills or Hows” on the General Geological Map which

accompanies his Bulletin His own descriptions reter only to dykes cuttin the

tron Mouarch orebody, and he quotes G. H. Taylor's deseription of a spevinin

asd pvsoxene dolerite”. On the map, lowever. Were is shown an outcrop three

miles by to riles. around Old Roaopena Hs. (10 iniles east of Tron Knob)

and in ain appendix Tavlor describes three specimens frou this area as vesicular

hasultic lavas. Specimens since collected are scarcely distinguishable in the

hand specimen from the most common amygdalatdal trachyte of Wooltana and

nie been described by Funder us exact equivalents of the Wooltana rocks, Tut

tar less wHeeted by subseqnent chanytes. The hivas are overlain by a eonslomer-

ate Tapped us Corvona conglomerate, containing pebbles of volcanics.

Mount Remarkable

Mount Remarkable, 30 qutles northeeast of Port Pine, Lorms i precipitons

scarp, 2,000 fect above the Willochta Plains, ts structure was examined by

Hawehin (1916) and found to be camplex, there heing strong meridional

{qutting and crushing, the sudden ending of the range being attributed to

east-west faults.

In the “Foot Hills” between the southern end of the scarp ridge and the

town of Melrose at its buse to the east is an area ol erushed limestones and

THE WOOLTANA VOLCANIC BELT, $A. WT

ribbon shites (above a tillite) in whieh Wowehin stated that numerous small

plays and pipes of basie igneous rock, with a few acid types, occur over an

aren about one mile by half a mile,

Fh. O, Thiele (1916, in Howchin, 1916) deserihed these rocks as of three

types: (i) altered dolerites, (i) quarte porphyries (including “quartz-veru-

tophyre”), Gii) wplites. He compared the first gronjs with the Blinnan basic

rocks, From his Spneyttians it seems likely that the “quartz-ceratophyre” very

strongly resembles the porplhiyritic sodic rfivelite of Wooltana,

It is suggested here from a review of the pnblished evidence that the Mount

Remarkable igneous eomplex is diapirvic.

Olary Province

Jones, Talbot and MeBriay (1962) suggest that rocks mapped on the

Plinbago one-mile sheet of the Geolugieal Survey of South Australia by Cain-

pani as “amphibolites, epidotes and skarn rocks” in Archaean rocks are volcanic

and that the sequence “probably represeuts a spilite-keratophyre assemblage

with interbedded shales”, They refer it to the Archwean, The authors kindly

showed specimens to the wriler: they ¢loscly resemble the more metamorpliosed

Wooltana rocks. Tt is suggested here thal (hese racks are of Willouran are.

Those near the southern boundary of the Plumbago sheet occupy a svueline and

we mipped by Campana as overlying his nppermost Archaean, and uncontorm-

ubly covered by Sturtian. "Those of the Jarger outerop extending eust-north-cast

from daghes prospect could be intrusive info Campana’s Archaean and are

mapped as uncontormably covered by the Torrensian Series.

Nee Sonth Wales

Barrier Ranges. According to Bo P. Thomson discontinuous onteraps of

lavas oceur in Adelaide System rocks (Torrowangee Series) from about 30 niiles

north of Broken Hill ter a distance of at least eight miles, continuing to the

north (King and Thomsen, 1953. p, 347 and personal communication). ‘These

vecur ulong a folded and Jocully fanited zone, which could explain the dis:

continuity. They were described as altered amyydaloidal and vesieular basilts,

A specimen kindly presented by Mr. Thomson was described by M. J, Bucknell

5 an umygdalaidal quartz andesite,

The lavas overlie thir beds of liniestone, sandstene and grit whieh -them-

selves ameonlormably overlie the Willyumu Series. ‘The contact between the

lives and an overlying tillite Gwhich contains erratics of voleanics obviously of

local origin) as disconformable,

West Darling District, In Keamy (1939) Javas (felesparporphyry and

rhyolite), interhedded with sediments whieh aceording to Thomson (pers.

conn.) are probably of Adelaide System age, are recorded in the Gnalta-

Grasmere area (80 miles northeeist of Broken ill). Speeimens callectect fy

the present wuthor in L961 ineInde some closely resembling Wooltana havin.

Green tiffaceuus sandstones of similar dee wre recorded near the Coppermine

Range (100 miles north-east of Broken Hill). Porphyry and delsite Java flows

ocenr in thé Cootiwundy Hills to the south of the Coppermine Range, ‘The

distribution of these onterops bas aw northavest trend in syrapathy with a

revionial fault direction (the Wioratta-Kucnenberry Fault of King and Thomson

p. 559) which is associated with wold and copper mineralization.

At Mount Arrowsmith (125 ailes north of Broken Hill) andesite and

amvedaloidal basalt were recorded by Kenny (p. 54) “and appewe to be ar-

ranged as lava flows about a centre of voleanic activity more or less eentem-

14h Rh. CRAWFORD

poraneous with the upper beds of the Torrowangee Series. These ancient basalts

have undergone considerable alteration, epidote being very common in veins

and irregular masses within the basic lavas. The general trend of the main

structures is north 30 degrees west”, parallel to the general direction of the

Waridtta-Koouenberry Fault,

In the Waratta Ranges (180 miles north of Broken Hill) Kenny recorded

flows of felsite and porphyry interbedded with sediments and equivalent in

age to those previously incutioned, Possible volcanics of similar age occur in

the Scopes Range (50 miles east of Broken Hill), 1

it is noteworthy that tillites were recorded in the Koonenberry Gaz close

to the top of the ‘Torrewangee Scrics.

Far North of South Australia —Indulkana Ranges

In the extreme north of South Australia Proterozoic outeraps are rare, hit

west of Granite Downs ILS, in the Indulkana Ranges an area ot “vesicular

basalt and melaphyre” has been mapped south of Chambers Blufl by Spriyy,

Wilson and Coats (1956) on the Chandler one-mile sheet. These are shown

as averlying Sturtian tillite. A smaller aren is mapped 20 miles east, near

Wantupella swamp, at a similar horizon.

Northern Territory

Protcrozoie voleinies are widespread in the northern Territory. Hossteld

(1953) gave the name Aygicondi Series to rocks assigned to this age, and stated

(p 114) that they consisted originally of “arenaceous and argillacenus sedi-

ments with a considerable amonut of tuffaceons material and very few calcurcous

deposits", the tuffaceons matcrial having been subsequently metamorphosed to

schist. Hossfeld rewarded certain rocks at Hatches Creck as of this age; these

contain amygdaloidal lavas, Toffs of the Pine Creek district he regarded as

sugecstive of “original lavas of intermediate composition, dacites or andesites,

but probably the latter”.

Regional mapping by Bureau of Mineral Resourees geologists has since

confirmed the widespread occurrence of Proterozoic amygdaloidal rocks.

Examples of these collected [rom the Edith River voleanics (Katherine-Darwin

regign) were stated to resemble Willonran voleanics (Webb, 1959). As Finder

pots out in the accompanying petrological notes, valceanies collected by

Bureau of Mineral Resources geoloyists in the McArthur River Basin on the

gentth-west side of the Gulf of Carpentaria are practically identical with the

Wooltana rocks.

Noakes (1957, tuble, p. 224) refers the Wollogoraug volcanics of the Gulf

of Carpentaria-Barkly Tableland area to a Willouran-Torrensian horivan,

Western Queensland-Monnt Isa

Knight (1953), discussmg the regional geology of Mount Tsa, mentions

amyedaloidal rocks and tufls in the Greenstones Group. This is the lowest

Group of the Mount Isa Serics according tu Jones (1953), who places it in the

Proterozvic,

Western Australia

David and Browne (1950) correlated the Nullaginc Series of Western

Australia with the upper Adelaide Series (System) of South Australia. The

basal bed, 300 feet thick at Nullagine, they accepted as fluvioglacial, quoting a

correlation with the Staruan by Becher in 1898.

THE WOOLTANA VOLCANIC BEET. S.A, 1-49

Browne stutes (p. 73) that in the Pilbara Goldfleld “contemporaneous

voleanic activity is strongly represeuted by acid, mtermediute and basic laya-

Hows and pyroclastic rocks, These are in places at the very base of the sorics,

but may be interbedded with the sediments on more than one horizon... Thick

felsite Hows arc present... . Numerous volcanic vents have been found, sur-

sounded by coarse ugvlomerates, ‘tnffy amd vesicular and amygdaloidal lavas.”

In the ‘Townsend Range a series of that nume. equated with the Nullagine

Suries. ineludes allered vesicular Javas in its lower part, and lavas are common

in the Kimberley Division Nullagine Series, Noakes (1957) refers the Morn-

ington volcanics of the Kimberley Plateau to a lower Torrensian horizon.

CONCLUSIONS

WoolTANA AREA

Mapping of the Wooltana Voleanic Belt shows that at least 2,000 fect of

Javas and associated pyroclastics of Willonran age outcrop aver ai area ubout

15 miles by 5 miles. In the immediate district it seems probable that north-

witrds ane westwirds they thin aud a change to a more sedimentary facies Is

nusked by metamorphism. Southwurds and eastwards there is insufficient

evidence ta slute whether they are concualed or absent. The major part of the

outerop jies along an important lineament forming the castern limit of the

Flinders Ranges,

The volcanics are overlain disconformabiy by Torretisian sediments which,

near Wooltana, are thin or absent but which thicken rapidly to the north and

west. These are unconformably pverlain by the Sturtian lower vlacial sequence,

which near Wooltana rests directly on the voleanics, -

The area is bisected by a major meridional structure, the Paralana Fault,

which has a throw of over 20,000 feet. Intense splinter-faults, wrenches and

thrusts are associated with this and caused ubiqnitous breceiation, Tight folding

occurs in the north and west.

Petrographic examination ot the volcanic rocks show that they are mostly

trachytes, with yery subsiciary porphyritic rhyolite and some andesite. The

trachytes arc sodie and wousual in being rich in haematite and are often amygda-

loidal av vesicular,

The presence of interbedded though thin sediments of shallow-water type

suugests that same Hows at least were submarine. No pillaw lavas have been

found and most of the volcanics are of sub-acrial deposition. Some filled up

shallow waters and others were temporarily submerged and covered by water-

deposited sediments,

Vhe Woultana volcanics uppesr mustly to have been extruded from fissures,

of which the inain lineament along the Wooltana scarp foot was probably

much the most important. Central vents are few and small.

‘The association of volcanics with lineaments often known to be faults, to-

gether with the combination of predominantly sub-erial effusion with some

shallow water sedimentation has been explained experimentally by E. S$.

O'Driscoll (pers. comm,), In producing domes and basins by shear foldine

techniques he has demonstrated that the hingeline is a uadal Tine which eyin-

hines the zone of maximum weakness with the meeting point of ground, air

and water. Further, it defines the locus of maximum shear, maximum delorrna-

130, R. CRAWFORD

lion dnd maximum rate of change of attitude, with all the attendant masima of

sedimentation rate, turbidites, fracture, breeciation and, in the inclined shear.

overturning and thrusting:

The fissure effusion of the voleanies could, theretore, be associated cither

with a prominent scarp due to bluck faulting or with a lincament showing nu

marked relict. Any present day relief along such a Tineument would have, of

colirse, mo necessary relevance to the environment al the time of efusior,

Dorme

Baslh )

Water

FISSUPEC SOUPCE

Fig. 4. Sketch showing relationship of voluanie fissure of Wooltana Lype to hinge-line

hetween dome anc hasin.

Abin ink GrosyNCLinr,

The known occurrence ol similar rocks in sifee and in diapirs elsewhere in

the Adelaide geosyncline suggests that either the original area of effusion was

Very much larger, or that other scattered aueurrences. exist, mostly naw cun-

eeuled. Because the erasion during and immediately preceding Sturtian time

Was intense but apparently local, the second suggestion seems more probable.

ven if only the northern half of the geosyneline is considered (i.e. abont

as fer south ag the southernmost known related rocks at Mount Remarkable )

aun arca of 30,000-40,000 square milus may have been affected. Whiether this

was ever a complete caver of lavas or was in discontinuous but extensive spreads

from Jocal centres is uncertain. The Wonltana oectrrence could itself be such

ti local centre, related to the known linear weakness along the Wooltana searp

foot. This could apply also to the Depot Creek (Wilkatana) occurrence, itself

on a qiajor fault. The almost invariable occurrence of Willouran volcanics in

unmerous diapirs ut first sight suggests a complete coverage. Bnt as the age

of the beginning of doming at Blinman has been shown by Coats (pers. eet.)

ta be probably contemporaneous with Sturtian deposition, and as this coming

may be the first surface expressian of diapirism, it is possible that the dinpirs

are located on ventres of volcanic activity which started in Willouran time and

continued long after it, rather than local revelations of what lies everywhere

below. Although there is na evidence of post-Willouran valcanism at Blinman,

other occurrences exist, e.g. at Chambers Bhiff (Indulkana sheet) which conld

come within this category, There is also uo certainty that some necks at Wool

tana are not post-Willouran,

Winrn AusTRALIAN Corre Avion

The oecurrence of preciscly similar rouks at similar stratigraphic horizons

in various distant localities, including Tennant Creek, N.T. (S00 miles. north-

north-west of Woollana) and Bauhinia Downs, N.T, (950 miles north) as well

GEOLOGICAL MAP OF

WOOLTANA VOLCANIC BELT

A, R.CRAWFORD

GEOLOGICAL SURVEY OF SOUTH AUSTRALIA

BArkarcols Bore

ou/der Bo,

Woodlamulka Mine Gu

as v Vv $

ye Vi v, _— =

) ‘a

Poe Me Ch fo "

M1 JACOB “4S

tare HAS,

STRATIGRAPHIC COLUMNS

DARAARA HA WORTH EAST. WOOL TANA

GORGE (nAnanools CAFES) MOUNT JACOB

WUNYALIINA VALLEY

STURTIAN

TORRENSIAH

Aniline

Syachee

Taree Fauins

Wereneer faults

Orhrer Faults

Sreike enird ay in tageted

WILLOURAN

NOTE

COPPER MINERALIZATION:..-.. Cu, varnee?

GOLD MINERALIZATION

SPECIMEN LOCATION WITH THIM SECTION WO _ ssze Pagmerires

Borecerp

Quart: & [ean Blows

~ ah» |

WETRES 2000

‘Trans. Roy, Soe. S.A, Vol 87, tig. 5. Qeglosies! Map of Wooltana Voleanie Belt,

THE WOOLTANA VOLOANIC BRET S.A, 1G!

as very similar rucks from almost certainty the same horizon over lurge prrls

of Western Australia, western New South Wales and westeru Queensland is

of great interest. Making dur allowance for erosional losses in a well-yjuthen

ticated Australian-wide Upper Protevogoie glaciation and a widespread Permian

glaciation, it seems reasonable to postulate an effusion of Proterozvie voleanics

of Willouran age comparable, if not so continuous in extent, with the classic

food basalts such as the Deccin Traps, Drakensbergs and Keeweenawans-

Restricting discussion to South Australia and the adjacent areas, lack of

knowledge of the lasernent geology of the great sedimentary basing and ot

those parts of the massifs masked by Quaternary deposits prevents even at

approxiuate ussesyinent oF the veal relationships with (for example) western

New South Wales.

Acmajor problem in South Australia is the age amd structure of the vast arca

of igneous rocks known loosely as thy Gawler Range porphyry. This not only

forms the Gawler Rages as shown on most maps, but extends far to the north

aod is known near Kingoonya, at Tareoola, und for 100 miles north, Jack (1917)

regarded it as an effusive lying on the Archacum gueisses. No study of the

porphyry itself has yet been made. Much confusion about its age has urisen

bucwise of the discovery by Jack, repeated by Mawson (1947) of pebbles al

Gawler Hange porpliyry tvpe rocks in dn arenaceous formation (Corunna con-

wlomerule) lving east of the porphyry mass und af uncertain relation both wilh

it wid with Olhey rocks in the geosyncline, where Sturtian glacial beds corticin

orratics OL similar porhyry; and the discovery by Johns aud Solomon (1955)

of intrusions of Gawler Rarge porphyry in that same arenaceous formation,

At the time this paper wes submitte:t in its original Form ay a thesis the

problems was uusolved. The anther suggested then a genetic relationship

between the Gawler Range porphyry and the Wooltana und other equivalent

voleanies. At tat tie he was particukaly strack by the similarity between

the sequence of events in the Isrongo complex of South-West Africa (Cloos,

L919) and a possible though onproved sequence in northern Eyre Peninsula.

This, loxether with the petrograplie similarity of the “boral porphyry" of

Merinjina, Wooltana (7.8. 5265) and specimens of Gawler Runge porpliyry

led him to sugeest that the Gawler Range porphyry is “aun aiusive mass formerly

covered by, and possibly bing on, a lava of which the Wooltany and. athe

voleanics are local remnants of the floods spreading further oul (possibly, at

Wooltana itsel!, lowly more abundant extvuded). This porphyry-lava camplex

could be... a larger version of the Kronge complex of South-West Africa

(Gloos, 1919). Lt would sitee have heen deprived of its outer skin on the upper

surface by erosion, ‘The relatively miter oecurretices of porphyry at Wooltana

wid their apparent equivalents (e.g. at Mount Remarkable) having been de-

rived from a similar ultimate source”. Tt was further sugvested that the intru-

sions of the Gawler Range porphyry into the Corunna conglomerate were a late

phase (it should be voted that these lie well east ol the main outerop of ithe

porphyry) and, following Jaok, that the Moonta Porphyry was also gonetioall

related, and was possibly a deeply eroded feeder.

The economic importance of a study on these lines was erojlnisized, the

Woallana volownies having copper and gold mineralization, and cansidered

with the Gawler Range Porphyry to be the ullimate source of the widy-

spread) copper mineralization of the Flinders Ranges, and the Moonta

Porphyry being known to be the host vouk for very rich copper lodes. While

the mineralization actually in the Wooltana voleanies and the two: porphwrics

is, af cOurse, magmatic (if often structurally controlled) it is sugyusted that

152, fl. CRAWFORD

much of that in the Adelaide System sediments is of the submarine exhalative-

sedimentary type (Ofteduhl, 1958). The widespread distribution of copper

and other minerals in sediments known to occur in extensive basing crossed

by numerous linewments along whieh volcanics oceur suggests that gas emission

accompanying the volcanic lavas and tuffs caused chemical reaction with sea-

water which by marine circulation led to mineral deposition fur beyond the

cmission ares.

In 1961 & sirmous traverse of the Gawler Range porphyry outerop and

surrounding areas was made with B. P, Webb and J. Johnson. The discovery

that the reeks at Roopena included by Miles in his “Younger Dolerite” suite are

identical with the typleal Wooltana amygdaloidal trachyies gave immediate

encouragement. The discovery of definite extrusive rocks (volcanic breceiu,

voleanic¢ glass and taff) at one of Johns and Solomon's intrusions and elsewhere

follawed. It was immediately evident that the “Gawler Range porplivry’,

though possessing a very strong identity m that red porphyritic sodic rhyolites

ure by far the cummonest rocks, is uevertheless a great volcanic complex.

Tn a report-on this reconnaissance the fact that the gold and tin mineralizu-

tion at Glenloth and Tareoola is closely ussuciated with variants of the lypicul

Gawler Bange porphiyritic rhyolites was cmphasized.

The author's later discovery of huge intersecting circular structures up to

35 miles in diameter (possibly 50 miles) and definite central vents parasitic to

these, both associated with major straivht lineaments snewests that both cir-

cular and straight fissures were the major sources of a vast but quiet ellusion of

rhyolite leva in the Gawler Ranges, with local explosive central vents. The

relationship of this to the Wooltana, Oraparinna, Roopena and other trachytes,

though certainly genetic, needs further study.

ACKNOWLEDGMENTS

The author thuuks his Geolagical Survey colleagues R. P. Coats (whe has

mapped mach of the rest of the sheet), R. C. Horwitz, D, Thatcher, B. P.

Thamson and B. P. Webb. TH. W Pander bas been especially helpful in the

petrology. Professor A. BR. Alderman has been an understanding supervisor.

Miss A. K, Brook, Mr. W, Rossini and Mr, B. Tink produced elegant copivs

of the author's original maps. Acknowledgment is due to Mr. and Mrs. |. Ford

OF Wooltana for Lospitulity, The authar thanks the Director of Mines, Suuth

Anstralia, for permission to submit Departmental work for publication.

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Croos, F., 1919. Der Erongo, Beit Z. geol. Erforseh. Deut. Schutzuel., 17, 1.

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THE WOOLTANA VOLCANIC BELT, S.A, 153

Dickrson, B,, 1953. Copper Deposits of the Northern Tlinders Ranges, Geoloey af

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Howes, W., 1916. Geology of the Mount Remarkible Arca. Trans. Roy. Soc. $. Aust,

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Tlawerry, W,. 1922, A Geological Traverse of the Flinders Ranges from the Parachilna

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Jack, R. Loexianr, 1917. The Geology of the Mooutt and Wallaroo Mining District. S.

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Jones, J. G., Tarpot, J, T,, and MeBsran, E. M., 1962. A Suite af Voleanic Nocks with

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Mawson, D., 1912. Pre-Canmbrian Areas In the North-asteri Fortien of South Australia

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Mawson, D,, 1948. The Proterozvic Glacial Record of the Bibliando Dome, Proce. Roy.

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Mawson, D:., 1949. Sturtian 'Tillite of Mowmi Jacob and Mount Warren Hastings, North

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154 R. CRAWFORD

Noakes, L, C., 1957. Upper Proterozoic and Sub-Cambrian Rocks in Anstralia, In Opik,

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Region. S. Aust, Dept, Mines Geol. Surv. Unpub. Report.

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Neighbourhood of Wooltuna Station. Proc. Roy. Soc. N.S.W., GO, pp. 283-304,

APPENDIX

Analyses of Wooltana yolcanie rocks by H. W, Sears, Australian Mineral Developinent Labora-

tovive. Specitie Gravities by Geophysical Section, Geolagical Survey, of South Australia.

Epidotizet trachute Trochyte

Wooltana: Woodnamoka Wooltima: Triangle

Well of Voloanios

(J'S,3228) ;

AIO, 53-2

ALO, 12-8

reo.O, 10-92

Ped (0-77

Mz0 2-36 |

CaO 15-8 '

NaO 0-1

KO 0-15

HA) — (al

H,0 F (84

COs 0-71

Tis 1-42

POs 0-18

SOg Nil j

Cl Nil

MnO U-l4 H

nr 0-03 | —

Specific Gravity 2-86 2:75

Puate 1

R. CrawForp

*BUISSOIO

your, [eUL vuRpeIeg plo yw Yyaesp TPM Pyoureupoo AA ay{yorsy

vjoorypry ‘odgory oArssePy “GAT = |eplopepsdAure pur aymosoA f SET

‘xefduiog Jeyueg pur yegq oruvojoA,

LuRPOOAA JO Jaed usOYQIOW pue [eyUd.

jo “YqIou Burpooy “Ma Iny 'g “AI

“SH, vue.

FOOAA JO JSaM ApoyeIpOUItuty

“‘aqAyoryy [epropepsAtue peodAy, “¢ “BI

Pq ommvspoA, LurzOO AA,

TOAD “YNos BuPOo] ‘MOIA ITY CT Bh

“Trans. Roy. Soc. S.A.”, Vol. 87.

R. CraAwForpD

Fig. 1, Barraranna Gorge. South

Fig. 2.

View of area west of Paralana fault looking north to

Mount Painter (the prominent monadnock).

Fig. 3. Close-up

“Trans. Roy. Soc. §.A.”, Vol. 87.

of Sturtian lower glacial formation,

Merinjina Creek.

PLATE

THE WOOLTANA LAVAS

BY H. W. FANDER

Summary

The geological setting of these rocks is described elsewhere by A. R. Crawford. The petrography of

the Wooltana lavas is unusual and distinctive, and is given in detail. Comparisons are made with

similar rocks from other localities in South Australia, and some evidence is presented showing

correlation between the Wooltana rocks and similar material occurring in widely scattered parts of

the Northern Territory and New South Wales.

TUE WOOLTANA LAVAS

by H.W. Faxpen®

[Read 11 Apri] 1963]

SUMMARY

The ecological setting of these rocks is described elsewhere hy A. BR. Craw-

ford. The petrography of the Wooltana lavas is unustal and distinctive, and

is given in detail, Comparisons are made with similar rocks [rom ather localities

in South Australia, and. some evidence is presented showing correlation belweeu

the Wooltana rocks and similar material occurring in widely scattered parts of

the Northern ‘Verritory and New Sonth Wales.

INTRODUCTION

The Wooltana lavas present problems Gf classification, owing to their unusul

texture and constitution. Compositional yariations and successive stages of

alteration have further obseured the picture. However, the distinctive nature of

these rocks has aided their comparison and correlation with certain other rocks

aceurring at Roopena (10m. east Of Lion Knob) and at Depot Creek (Southern

Flinders Ranges). The pyroclastic deposits associated with the Wooltana lavas

contain Fraginents of sodic rhyolites strikingly similar lo some of the Gawler

Range Porphyry types; this fact opens up interesting possibilities of petragenetic

links between all the areas concerned. The Gawler Range Porphyry itself shows

compositional variations ranging from andesite through trachyte to sodic

rhyolite,

1. THE WOOLTANA ROCKS

The main rock-type represented in the igneous sequcnee in the Wooltana

itrea is a red to black or purplish, amygdaloidal extcusive rock. The amygdales

often have a selvedge of pink feldspar and are filled with quartz. The macro-

scopic appearance of the rock is thus quite distinctive.

In thin-section, the freshest samples of the lavas consist of laths of feldspar,

randomly embedded in massive, fine-grained lemutite. The feldspar has been

carefully studied by mineralogical means and by X-ray diffraction, and is

thought to be a member of the sanidine-wnorthoclase series, probably in most

instances nearer to the anorthoclase end, The usual range of dimensions of

laths is between 0-04 mm. % 0-20 mm. and 0-08 mm, * 0-40 mm. In some

thin-sections, pscudomorphs of iran-ore suid antigorite oecur which hy their

shape and constitution suggest that they represent completely altered micro-

phenocrysts of olivine, The amygdales are typically lined with euhedral

crystals of reddish microcline and filled with quartz and calcite. In some in-

stinees, pure albite or chlorite occurs as fillings, but a microcline lining is almost

Trims. Roy, Soc. §, Aust, (1963), Vol. 87,

156 i. W. FANDER

More altered rocks show replacement of feldspar Jaths by quartz, in paleles

showing sirimitaneons extinction unrelated to the orientation of the laths. In

other instances, particularly in more seoriaceons types, the microcline hus veined

the rack and partially replaced original feldspar, as well as lining the amycdales.

Secondary or late-stage introduction of minerals, which postdates the filling

of the amygdales, has occurred in successive stages, An earlicr stage involve

the introduction of muscovite and quartz, accompanied in sume instances by

little tourmaline und phlogopite. This ix a siliceous, potassic phase. A later

stage was dominantly ealcic, introducing fibrous tremolitc, caleite, sphene.

epidete, and finally scapolite. The (remolite, epidote and seapolite veer in the

hody of the rock, but the other minerals are to be found in the amygdales. In

places, the tremolite, seapolite and epidote have so obliterated the original

stueture that very little resemblance between the altered and the fresh ravks

remmains,

The texture of the fresh rock is distinctive and unusual. Although the rock

must he classified us u trachyte on the grounds of its mineral composition. its

texture is not trachytic; fow-strncture is couspicuons by its absence, The

feature: could more uceurately be deseribed as slagey, consisting of random to

sub-vadiating laths ot feldspar in hematite; the amvedales are often rimmed with

massive hematite containing practically no feldspar. ‘This is probably due to

more rapid cooling adjacent to the original, unfilled vesicles. The slagev texture,

brought about by very rapid chilling of the rock, is in keeping with other von-

siderations such as the general absence of primary ferromagnesian minerals.

aml the presence of the high-temperature feldspar (anorthoclase). The prob-

able former presence of olivine is also significant in this regard, since this mineral

does not normally occur in acid to intermediate rocks except in the sapidly-

cooled estrusives where the matural sequence of Bowen's Reaction Series Ins

been arrested.

The hematite which forms such a large part of the trachyte is considered

to be primary; it occurs as dense aggregates and swarms of yery small euhedral

lw subhedral crystals, nsually denser adjacent to amyedales. Nowhere does the

hematite replace feldspar or any other mineral, Tt does nat oceur in the amyy-

dules. nor in Veins. Tt is not associated with the potassic, siliceous or caleic

secondary minerals described above.

Minor variants: of the Wonltana trachyte include slightly coarser-grained

microsyenites, and more caleic varieties classified as microdiorites. Hematite ix

abundant in all these, They are not usually amyedaloidal, and they reflect a

slower cooling history and slight differences in the composition of the magma.

The associated pyroclastic rocks are lithic Udfs and lapilli-tuffs, They con-

twin fragments of Wooltama-type Gachyte and of sudie rhyolite remarkably

similar to a widespread member of the Gawler Range Voleanic Complex, In-

clusions of both these types in the pyrnelasts indicates their extrusion prior to

at least some of the volcanic activity giving rise to these deposits.

2. COMPARISONS AND CORRELATIONS

a. The Gawler Range Voleanic Coniplex

This comprises a range of igneous rocks, predominantly extrusive, extending

from trachyte and andesite to sodi¢ rhyolite and obsidian. This vast complex is

chunuelerized by the conspicuous and uniform reddening (sometimes termed

“magmatic reddening”) of its various representatives due to finely-divided

THE WOOLTANA LAVAS, S.A. 157

hematite. Extensive but as yet incomplete studies of the Complex strongly

indicate, on petrogenetic grounds, that the Wooltana Layas quite probably

represent a local variant of the parent magma responsible for the whole Com-

plex. The presence of Gawler Range rhyolite fragments in Wooltana lithic

tufls considerably strengthens this contention,

b. Depot Creek Voleanics

These racks strongly resemble the Wooltana Layas in every feature, being

only slightly coarser-grained and less hematitic. ‘The nature and mineralogy

of the alteration is closely similar to that of the Wooltana rocks. There is very

little room for doubt that both rocks had a common origin.

ce. Roopena Lavas

These rocks are remarkably similar to the Wooltana rocks in every detail.

Secondary ulteration is far less prevalent, heing mainly confined to sccondary

or late-stage muscovite. In some parts of the rock, the amygdales are lined with

pale chlorite, but the characteristic euhedral microcline is very widespread.

Qccasional microphenocrysts of probable sanidine-anorthoclase occur. There

is nu doubt that the Roopena and Wooltana lavas have a common origin.

d. Gnalta Area, N.S.W,

Porphyritic sodic rhyolites and trachytes occurring in this area may be

petrogenetically linked with the Wooltana lavas. Little is known about these

rocks as yet and thus detailed comparisons must be made al a later stage.

e, Northern Territory

Rocks very closely resembling the Wooltana lavas in petrogenesis and petro-

graphy oceur in the Borroloola area, the Hodgson Downs and the Bauhinia

Downs four-mile areas. There is a possibility that voleanic rocks at Tennant

Creek and Hall’s Creek may also be related. Extensive further investigations

are peedes to explore this concept which extends from Armhem Land to Eyre

eninsula.

Puatre |

H. W. FANpER

Vig. 2. Portion of a vesicle, showing

fibrous, cloudy microline; twinned,

Clear albite; and quartz. Crossed

polarizers. x 100,

L. The photomicrograph shows

sheaves of fibrous tremolite and a

pseudomorph atter olivine composed

of antigorite and yeothite. x 35,

Vig.

Fie. 3. Wooltana trachyte, showing Fig, 4. Typical texture of Wooltana

feldspar Jaths and hematite. Note trachyte. Laths of feldspar and

concentration of hematite surround- patches of serpophitic alteration pro-

ducts embedded in hematite. 33

ing microcline-filed vesicle in centre.

x G0.

“Trans. Roy. Soc, S-A.’, Vol. $7.

STONYFELL QUARTZITE: DESCRIPTIVE STRATIGRAPHY AND

PETROGRAPHY OF THE TYPE SECTION

BY G. R. HEATH

Summary

A detailed study of the Stonytell Quartzite in the type area disclosed the presence of 830' of

dominantly arenaceous sediments, The principal rock types are poorly sorted, somewhat calcareous,

felspathic greywackes and clean, well sorted and subarkoses. The sediments occurring through the

type section show sufficient variation to justify some reclassification and subdivision of the

Stonyfell Quartzite as a stratigraphic unit.

STONYFELL QUARTZITE; DESCRIPTIVE STRATIGRAPHY AND

PETROGRAPHY OF THE TYPE SECTION

by G. R. HeatH

[Read 11 April 1963]

SUMMARY

A detailed study of the Stonyfell Quartvite in the type area disclosed the

presence of S30’ of deaminantly arenaceous secliments, The principal rack types

tire poorly sorted, sormewhat culeareaus, felspathie greywackes and clean, well-

sortec| urkoses and subarkases,

The sediments ogeurring through the type seation show suffvient variation

to justify some reclassiteation and subdivision of the Stonyfell Quartzite as a

strativraphic unit.

INTRODUCTION

The Stonyfell Quartzite is the sixth Formation in the Torrensian Series of

the Adelaide System (Mawson and Sprigg, 1950). Lt outcrops along the western

edge of the Mount Lofty Ranges, east of Adelaide. as a series of “blocks”,

which are the faulted remnants of an original continuous occurrence, These

vutcrops are generally less than eight synare miles in area and ure separated

by faults which have a variable, roughly vorth-easterly strike.

To the west, the occurrences are terminated by the Eden Fault, producing

the well-defined searp which forms the western limit of the Ranges sauth of

Hope Valley.

OF the fault blocks, the one forming the prominent east-west ridge above

Stonyfell has been chosen as the type oceurrence of the Formation (Mawson

und Sprigg, 1950),

TYPE SECTION

The type area does vot contain an uninterrupted, well-exposed section

through the Stonyfell Quartzite, due to the deep weathering which hus affected

the ridge tops in this area, In order to obtain relatively unaltered samples

throughout the unit, the type section was measured in two purts.

The Jower beds were studied alone a spur, about half a mile cast of

Stonvfell Quarry (Jat. 34°55.25’S., long. 138°41.5’E., grid relerence 692534 to

693531, Adelaide 1:63,360 Militury Sheet). The upper part of the sequence is

well exposed in the south-east wall of Slapes Gully (lat. 34°37’S., long,

138"41/00.), wd was measured between grid retereuces 690821 and 690520, ~

Strativraplete: Sunemery

Top-4dlé? Thinky-bedded. well-sorted aml rennded subarkoses with aninor, shaley felspathie

gsreywicke parting,

41G-B8L" Schistose, felspathie greywackes interbedded with somewhit calcareous sub-

ar hoses,

GSL-S29" "Two quartzite sequences (651-738': subarkosic, TI0-$29": arkusie} separated) ly

schistoge wrevwackes similar to 416-681".

Trans. Roy. Soc. S. Aust, (1963), Vol. 87,

160

G, R. WEATH

Detailed Stratigraphy

Top-315"

213-335"

3335-416"

1141-4677

d67,524°

524-557

S37-U27"

627-68 1°

51-798"

738-THue

7FOQ B20°

Subarkoses; off-white 10 pule yellow-brown; medinm-groined; fuirly well sorted,

friable to sub-yuartvitic, with aniner (less than 20 qc.) arkoses. The clean

arenites, Which ste 2 in. to 2 fl thick, are separated by 3% in. shaley felspathie

geeywackes. Bedding is irreslar. and frecuently shows lensing and pinch unl

swell” structures. Low dip, planir eruss-hedding ts cormmon, Strength of oul

crop is generally poor to fair.

Of} white to red-brown subarkoses, simile to O2US witle abundant L in. Inter

bedded shaley felspathio groywackes, Bedding as 60-2157 Generylly crops out

poorly,

Subarkose; off-white to pale yollow-brown: anedinn-grained: fauly well sorteet:

dominantly snb-quurtzite to quurtzitic. Bediling js usually thin und irregular, but

is diffiendt ty see becanse of the homoeneity of the vnit and whsence of purting,

Cross-hedding is conmiou, The imit forms prominent outcrops, which shaw wood

rectanilar jomting and are commonly cuse-hardened,

Subarkoses; dominantly quactzitic; off-white: ty pale red-brown: fine- 40 pncedium-

vrained; poorly sorted.” Thinky interbedded with tilypathie greywackes: light grey

(o grey; fine- to medino-grained: pourly sorted: friable to subqnurtaitie; sclisluse:

somewhot caleareous. Bedding (ess than 1/10 in, ta 9 in, thick) is usnully

lrrevulur in thickness aad is commonly obscured by osuperiiipased sebistasity,

Suharkoses make up about two-thirds of the sequence. Strength of outerop is

fairly strony, due te the absence of well-developed jaint systems to assist mneelunteal

disintegration,

Interbedded snbarkoses awd greywuckes. Similar to 416-467%, bt ull bees vont

some caloite as mutrix or cement, Sybarkoses make wp about one-third of the

sequence. ‘The greywackes frequently contain irevular argillaceons laniinve

(? wd flakes) wud show irregular custerly dipping schistoyity, "The anit generally

crops out poorly.

Calcareous (average culeite eontent is about 14 p.c.) interbedded subarkases and

felspathie greywackes, generally similar ta 416-467%, Karns tuirly promineut out-

crops, which lave a “tlneky” appearance (due to the etching af jointed qnartzitic

beds), Subarkoses quuke a about bwe-thirds ef the seqnoneE,

Interhedded preywaekes aud modium-erained subarkoses, venerally sinilar te

467-524". Argillvecous hanainae are commen in the ereywackes. Subackoses muke

up at quarter tow third of the anit, Cenerally crops ont poody. However, a more

quurtzitic bed news the middle of the unit crops out fairly prominently in Shapes

Gully,

Arkoses; pink to purplish-grey; fine- to anediumeprniaeds generally quarteitio, inter-

bedded with felypathic greywaekess calcareous, grey to utey-ureen; schistose, Bed-

due, Tanging up to 3 1b, is generally thicker (han in the underlying wnits, Cross.

beceling is almost ubignitons, although obseared by erade, vasterly dipping

schistusity in some areas. Foresets range from lesy than 1 in, to 400r 30 {bin

length. ‘The unit crops out strougly in the vicinity of the type section, hut is not

as well exposed further oast.

Suburkoses and lesser arkosex; pale piuk fo light brown: fairly well to well sorted;

very dines ta meditun-grained, sub-quartzitic to quarizilie, Bedding ranges from

less Chan lin, to 3 ft, in thickness. It is dificult to see due ty the gradutional

variations in lithology, Rectangplar parting and jointing are very well developed,

‘Hw unit forms yery prominent outerops; the whole thickness commonly being ex-

posid as ve vertival cliff face.

Subarkoses; ealeareons; offavhite to pinkish; fine. to mediwo-gained; poorly

sorted; sub-quartzitic to quarlzitic. Tnterbedded with felspathic wreywackus, prev:

selistoxe; calcareous, fine to medium-geained: poorly sorted: friable to sub-

quartaitic, This secnence is sinilar to the interval 416-481 Beddine is genvrally

thin and irregular, Cross-bedding ig abundant. ‘Wie amit is venerally weil

exposed due to the protectian afforded by the enclosiny resistiint beds,

Arkose: olf-white to yellowish-brown ind occasionally pink; homogeneous; fine-

to inedium-grained: fairly well sorted; sub-quartzitic ta quartvitic, Sindarin

appearance to O81-738*. Bedding is generally tin. to 3 ft. thick and shows “pinch

ancl swell” structures. Jointing and parting are well developed, hut less perfectly

than 681-736". This umt crops out strongly in the type area Where it is commonly

exposed as u sub-vertical cliff face.

STONYFELL QUARTZITE 161

PETROGRAPHY

Principal Rock Types

Pctrologically, the rocks of the Stonyfell Quartzite fall into two well-defined

classes. Very few specimens show intermediate characteristics.

The most common rock type is a “clean” generally fairly quartzitie sub-

arkose, with an average mineral composition of 79-5 p.c. quartz and 20:5 pic.

potassic felspar (determined by grain count). Grains are well sorted, well

rounded and frequently have high sphericities. The most common cement is

silica, which has been deposited as optically continuous envelopes in the yoids

hetween quartz grains, Calcite cement was observed only in samples from the

middle of the formation.

The other common rock type is a poorly sorted felspathic greywacke, which

is Often somewhat calcareous and usually shows well-developed irregular

schistosity, The average mineral composition is 58-7 p.c. quartz, 12-0 p.e.

felspar (potassic varieties, with a fairly large proportion of sodic plagioclase

in the finer grain sizes), 20-7 p.c. matrix and 8°6 p.c, caleile (determined by

modal analysis), Grains are usually angular and have low sphericities. Packing

tends to he very open, the interstices being filled with very fine-grained quartz-

sericite-chlorite matrix. Plate 2 is a photomicrograph of a thin scction cut from

a typical felspathic greywacke,

190

Ch) Saborkases

Below Bue. s § 32

(\ Ys

Vs Ae Los

) Arkoses 270%

Sitbor hoses

63(- 738°

Greyvwotks

sibarkos:

‘

vex ev 22 sat di

So /\/\ FX 3

0 10 20 Morrix 40 50 60 70

70 60 50 4e/sear 30 20 10 0

Fig. 1, Mineralogical composition of samples from the Stonyfell Quartzite.

162 G. R. HEATH

Grain Size Characteristics

Thin sections were used for all grain size studies, as samples could not

be effectively disaggregated for sieve analysis (Krumbein, 1935).

The average of the arithmetic mean grain diameters for all samples studied

(corrected for the random intersection of spherical grains by the plane of the

thin section) was 0:345 mm. Fig. 2 shows that this value is substantially

constant throughout the section, although deviations are most marked near the

top of the formation.

900

800

700

600

500

tt above lose a feer

ferg

100

0 o-t 02 O-3 o-4 0-5 0-6

Diarverer te PIF.

Fig. 2, Graph of variations in the corrected arithmetic mean grain size of

samples from the type section of the Stonyfell Quartzite.

STONYFELL QUARTZITE 163

The degree of sorting in samples from the two main rock types is markedly

different. The “clean” arenites (subarkoses and arkoses) have an average

standard deviation of about 0-6 Wentworth grades, whereas the value for the

greywacke is about 1-0. Cumulative curves for two typical clean arenites (A

and B) and two greywackes (C and D) are reproduced in Fig. 3. The grey-

wacke represented by curve “C” is one of x number showing a distinct bimodal

grain size distribution. Fig. 4, a histogram for the same sample, shows this

property more clearly,

8 iy

Cumulative Percent! (Numerical)

Grate Qameter te tatr.

Wie

Vig. 3. Cwmulative curves of grain size distribution in samples from the Stonyfell

Quartzite.

Heavy Minerals

Heavy mineral grains were arbitrarily defined as those which sank in

tetrabromovethane ($,G, 2-96). Non-opaque minerals covered by this definition

constituted 40 te 1,300 parts per million of the samples studied.

Six opaque and nine non-opaque minerals were identified. In addition,

optical propertics were used to subdivide rutile grains into three groups, zircons

into three groups, and tourmalines into 13 groups (Krumbein, 1946).

The opaque mincrals identified were haematite, ilmenite, leucoxene, limo-

nite, magnetite and pyrite, all of which were quite common, Of these, only the

ilmenite, magnetite and portion of the haematite and pyrile are considered to

be original detrital constituents.

The non-opaque minerals identified were andalusite, garnet (dominantly

almandine, with rare grossularite), monazite (rare), rutile (pale yellow, orange

and deep red varieties), sphene, spinel (rare), topaz, tourmaline (13 varieties,

164 CG. R. HEATH

including iron-, magnesium-, sodium- and lithium-rich, as well as intermediate

and zoned varieties) and zircon (the most abundant non-opaque heavy mineral,

usually pale pink, with a few highly spherical colourless and deep pink, pleo-

chroic grains), These minerals are all considered to be original detrital con-

stituents.

Ruamerteal Percent

] Yo V4 Ig ‘ig /32

Grate Lbieereler se pri,

Fig. 4. Histogram of grain size. distribution in a typical greywacke from

the Stonyfell Quartzite,

CONCLUSIONS

The Stonyfell Quartzite, in the type urea, consists of 830 ft. of dominantly

urenaceaus sediments.

This sequence has been defined as a Formation by Mawson and Sprigg

(1950) and has subsequently been mapped as a single unit in the Adelaide area

(eg. on Adelaide and Echunga 1-mile series geological maps ).

However, within the type area (which was mapped in detail to facilitate

the choice of a well-exposed section for detailed study), the sequence consists

of three well-defined units, with several quite persistent sub-units. These three

main units, as well as some of the sub-units, are also recognizable in other

Stonyfell Quartzite outcrops, which haye been examined by the author since

studying the type section. In general, the cleaner, more quartzilic arenites

are recognizable over a considerable area, whereas the schistuse greywackes

tend to grade laterally to finer-grained phyllites.

STONYFELL QUARTZITE 165

As a result of these observations, the following subdivisions of the Stonyfell

Quartzite (based on the type section) are proposed:

Interval in the

type section

Stonytell Sub-Group .. ss m 0’-829’

Wattle Park Formation - on 0’-4167

Member A G . 0-335’

Member B . 7 . 330’-4167

Slapes Gully Formation . 4167-681"

Greenhill Formation 4 « 6817-829’

Member A ; 2 . 681’-738'

Member B va _ 738'-790°

Member GC iF 7 . 7190’-829°

ACKNOWLEDGMENTS

I received assistance from several people and organisations during the

period of this research. Particular thanks are due to Professor A. R. Alderman

and Dr. R. L. Oliver, who supervised the project, and to Mr. L. G. Nixon, who

provided many enlightening discussions.

REFERENCES

Krauser, W. C., 1935. Thin section mechanical analysis of indurated sediments. J.

Ceology, 43, pp. 482-496.

Krumaers, W. C., 1946, Tourmaline group in sediments, J, Geology, 54, pp. 65-87.

Mawson, D., and Sprice, R. C., 1950. Subdivisions of the Adelaide System, Aust. Journ. Se..

13, pp. 69-73.

Nixon, L. G. B., 1961. Greenhill Quarrics. Min. Review, Adelaide, 111, pp, 122-124.

ot the Mount Lofty Ranges. Trans. Roy. Sac, S. Aust., 70, pp. 313-347. ;

Raccart, H, G,, 1959, Australian code of stratigraphic nemenclature (third edition), J.

Geol. Soc. Aust., 6, pp. 63-70,

spricc, R, C., 1946. Reconnaissance geological survey of portion of the Western Foothills

of the Mount Lofty Ranges, ‘frans. Roy, Soc. $. Aust., 70, pp. 313-347.

G, RY. TWeavn Povrh |

Hig 1 Upper members of the Stonyfell Quartvite overlain by plivllites, on the existern aici

of Slipes Gully. Looking east across Lone Ridwe to Mount Lotte, fron Stonyfell

Hig 2. Photorvierograph of a thin section from an angitir, very poorly sorted, relsputhic

ereywacke, Crossed nicols, x 120,

“Trans. Roy. Sac, S.A" Val. 87

THE GEOLOGY OF THE MOUNT CRAWFORD GRANITE GNEISS

AND ADJACENT METASEDIMENTS

BY KINGSLEY J. MILLS

Summary

The Mount Crawford Granite Gneiss, a small elongate body of gneiss near Williamstown, South

Australia, is considered to be the result of synkinematic granitisation of metasediments. This quartz-

microcline-albite-biotite gneiss is sharply bounded against the quartz-albite-sillimanite-mica schists

which it has replaced. A number of mica schist inclusions (skialiths) occur in the granite gneiss.

They show structural elements parallel with those of the nearby metasediments and have

gradational contacts with the gneiss. The minor heavy minerals of the granite gneiss are similar to

those of the metasediments. The zircons of the gneiss and the metasediments arc identical in size

and shape, with a distinct lack of euhedral form. A brief summary of the petrology of the

metasedimentary sequence adjacent to the granite gneiss is presented. A zone of retrograde

metamorphism and hydrothermal activity surrounding the granite gneiss appears to be related in

space and time to the granitisation. This zone is characterised by the presence of chlorite and

sericite (alteration products of original biotite and aluminosilicate minerals), and contains the

sillimanite, kyanite, clay and rutile deposits of the area. Intrusive rocks are amphibolites and

pegmatites. The amphibolites (metadolerites) form steeply dipping dykes cutting both the granite

gneiss and the sediments and are believed to be older than the granitisation. The pegmatites,

younger and unrelated to the granite gneiss, replace both the gneiss and the metasediments.

Complete chemical analyses of two garnets, a granite gneiss sample and an amphibolite sample are

presented. A study of foliation and lineation in the granite gneiss and adjacent schists, and joints in

the granite gneiss indicates a marked inhomogeneity of the structural elements.

THE GEOLOGY OF THE MOUNT CRAWFORD GRANITE GNEISS

AND ADJACENT METASEDIMENTS

by Kinestry jf. Minis

[Read 9 May 1963]

SUMMARY

The Mount Crawford Granite Gneiss, a small elonyate hody of gneiss near

Williamstown, South Australia, is considered to be the result of synkinenratte:

granitisvtion of metasedimonts. This cpuartz-microcline-albite-biotite yneigs is

sharply bounded upainst the quartz-albite-sillimanile-aniea schists which it has

replaced, A number of miea sehist inclusions (shialiths) ocenr in the granite

gneiss, Uhey show structural elements parallel with thase of the mearby ineta-

sedinwnts and have gradational contacts with the gneiss. he minor heavy

minerals of the granite gneiss are similar to those of the meutisediments. The

zircons Of the gneiss and the metusediments are identical in size and shape

with a distinet lack of cuhedrw] form. A brief summary of the petrology of the

metasedimentary sequence adjacent to the granite gneiss is presented. A zon:

af retrograde metamorphism aod hydrothermal activity surrounding the granite

wouiss appears to be related in space and time to the graniliyation. This zone

is characterised by the presence of chlorite and serieite (alteration prodnets

of original biotite and aluminosilicate minerals), and contains the sillimanite,

hyanite, clay and rutile deposits of the arca, Tutrusive rocks are amphibolites

and pesmatites. The arophiholitus (metadulerites) form steeply dipping dykes

entting hoth the granite gneiss and the sediwents and are helievtd to be older

than the granitisation, ‘The peymatites, younger and unrelated to the granite

gneiss, replace both the gneiss and ihe metasediments, Complete chemical

woalyses of two garnet. a granite emeiss sample and an amphibolite sample

are presented, A study of foliation andl lineation in the granile gneiss and

adjacent schists, and jomts in the granite gmeiss jidicates a marked inhomo-

geneity of the structural elements.

INTRODUCTION

The main vbject of this paper is to present and discuss the geolovical evi-

dence hearing an the origin of the Mount Crawford Granite Gneiss. For this

purpose an area of about nine square miles surrounding the granite gueiss was

studied. The area is situated on the Gawler (1 mch to 1 mile) Geological Sheet

south and west of the South Warren Reservoir, south of Williamstown on the

Williamstown-Birdwood road. This area is largely Crown Land; the castcrn

part being the western section of the Mount Crawford Pine Plantations, the

central part leased grazing land, and the western part steep virgin scrub country.

The topography has a relief variation of some 800 ft. the highest elevation

in the area being Warren Hill, just over 1,700 ft. This hill forms part of a

prominent north-south ridge in the centre of the area, dividing the relatively

matured uplands to the east from the more rugged erosion scarp of the

Kitchener fanlt to the west. Kast of the Warren Hill dividing ridge the gently

undulating slopes are commonly covered with original and reworked alluvium

and weathering products of the old uplifted Tertiary peneplain,

— Beng = = ae : =

Trans. Roy. Soc, §. Aust. (1963), Vol. 37.

168 KINGSLEY J. MILLS

This area was the site of the Mount Crawford Alluvial Goldfields which

were active in the late nineteenth century: Harry P. Woodward (1886), re-

porting on the gold drifts, was the first to diseuss the geology of the region.

Howechin (1926) considered that the metasediments. could be correlated with the

lower portion of the Adelaide System, a coarse cross-hedded pebhly sandstone

representing the Basal Conglomerate. Hossteld (1935) mapped the area and

regarded the cross-bedded sandstone as basal Proterozoic unconformably over-

lying Barossian (Archaean) schists and metasediments. He considered the

tranite gneiss Lo be the result of “pegmatisation”. Alderman (1942) studicd un

area immediately north of the present one and presented evidence for the produc-

tion by alumina metasomatism, of the massive sillimanite and kyanite rocks

there, He showed that the metasomatised zone was: rather Iseal and was

snrounded by metamorphosed racks. uf the bivtite grade of progressive regional

metamorphism, Campana and Whittle (1953) have emphasised the wetion of

metasomatism in the area with particular referenve to the origin of garnet,

rutile and aluminosilicate concentratious. Campana considered that alumina

metasomatism bas converted part of the hasal sandstone to mica schist,

Few small-scale bodies of metasormatie granite have been recorded in the

literature. Misch (1949) considered that metasomutie granites ocenr mainly

im a regional scale. Granitisation on a small scale appears to haye heen

neglected, and yet it is these small-scale examples of granitisation that are the

most useful in determining the causes and nature of Utis type af rock trans-

lormation.

The present mapping and petrological study was carried out in 1959 ind

early 1960 as a research project in the Department of Geology, University of

Adelaide.

STRATIGRAPHY AND METAMORPHISM

It appears that the stratigraphy of this area ean be correluted with the lower

parl of the Adelaide Svstein (Campana and Whittle, 1953). The rocks have

reached the amphibolite facies of regional metamorphism, and intense: reerystil-

ligation of the liner sediments to schists and cale-silicate rocks has almost com-

pletely obliterated the original hedding and other sedimentary features. Ay a

bolsequence no attempt was made to estimate original stratigraphic thicknesses.

Sedimentary features are generally well preserved in the sandstone members

of the sequence, however.

‘Lhe general stratigraphic sequence may be outlined as follaws:

Youngest. Cale-silicate group,

Mica schist vroup,

Upper tremolite rack.

Upper cross-bedded urkose.

Thick coarse mica schist sequence,

Lower tremolite ruck.

Lower cross-bedded sandstone.

Oldest. Sandy mica schists.

The spatial distribution of these stratigraphic units can be seen on the geolovieal

map.

Although the metamorphic facies appears to be constant throughout the

urea, the degree of recrystallisation (“intensity of metamorphism”, Chinner, 1955,

p. 44) varies considerably. The highest degree of recrystallisation occurs in the

coarse mica schist sequence near the granite gneiss and grades off towards the

6 SMUTH=

WaAwEN

Saf RAR

Kase Shh itate

Mec we SCHIST 3rR18

MPFED THENTIITE Ror &

COsMse GLawte woe soWesT te

FINE<GHAING S MICA Ath iD ‘%

TUFMOTLETES SOCR

| UPPER CAOde-BED

@HaAn|TE GKEISS

BSEHIST FNCLLS DN

WAtiTe SeHisST wWweLsical

GARNET WIGTIPTE SomIst

asebsiOn

COAREE MDa SOHIST STFA

WHKOSE

HYTPO tape Mey ATR RATION FORE

LOWER THEMML Fh MLC

, ERE SHaf4e mn ARETE

LOWES CAOS$-SECCED SaNOsTCuE

i BANOY MGA SerisTS

| RECMATETE [ se PO.

. *

f ANPHIiboiite 7 SILA MANITE BON /

GEOLOGY OF FOR TICAN

— aS a ——— an Tat

. a " ie MOUNT CRAWFORD |

DISTRICT

Seale ia Chan ‘9

Mg. 1. Geological Map of Mt. Grawlord District.

170 KINGSLEY J. MILLS

west. Metasediments above the upper tremulite bed, to the east of the grunite

yneiss, are much less reerystulised and this is attributed to the tremolite bed

acting as a local barrier to the metasomatism,

A futher complexity in the petrology of the metasediments is the presence

of a zone Of strong retrograde metamorphism and hvdrothermal activity sur-

Hindi the granite enciss. ‘This zone is recoynised by the alteration of biotite

to chlorite, and ot aluminosilicate minerals to fine-grained! sevicite (damaurite);

it extends west to the vicinity of Warren Hill, north and sonth out of the area

mapped, and is cut of to the cast by the Wwemolite rock hed mentioned abuve,

The granite gneiss and the rocks at its immediate contacts, constituting the ap-

parent centre of this altered zone, show none of these retrograde effects. the

siotite in these rocks being completely fresh. It is in the northern extension of

this zane of retrograde metamorphisin that the sillimanite, kyanite, rutile and

cluy deposits duseribed by Alderman (1942) are localised.

The Sandy Mica Schists which oeeupy the core of the complex anticlinal

sloicture in the western part of the area (Figs, 1 and 2) are the oldest rocks

recugnised, This anticlinal strneture has been named the Lookout Tower

Anticline (Campana, 1955). Although sedimentary structures have been almost

completely obliterated in these schists, grit bands containing detrital haematite

and occasional layers of pebbles define the bedding. The sninor folding is hest

displayed at the reservoir weir where it lms affected beds with alternating thin

quartzteldspar-rich bands and more micaceous Jayers. ;

The sandy mica schists vary from biotite-muscovite-rich varieties to mica-

venis arkoses in which only muscovite is present. The latter are difficult tu

distinguish from the overlyiny eross-hedded sandstone. Although Campana

(1953) regarded the sandy schisis as a melasomatie facies. variation of the

“basal” sandstone, the present authar prefers to regard them as a sedimentary

facies variation which stratigraphically underlies the sandstone.

The Lower Cross-bedded Sandstone surrounds the anticlinal core of sandy

mica schists. except on the castern side near Warren Hill (Pig, 1), where the

sundstane apparently lenses out. Cross-bedding, sometimes oecutring in thick

Festoons, is common throughout the sandstone and establishes it to be younzer

{han the sandy schists described above, The sandstone is a coarse, well-bedded,

friable, feldspathic rock, with detrital haematite spread throughout as well as

being concentrated in layers parallel! to the bedding planes. Small, rounded

aebbles are commonly found on the bedding planes. The pebbles are mostly

lavmatitic quartziles, but rarer quartz. pegmatite and quartz-tourmaline pebbles

are also present. Where folding is intense the pebbles have heen flattened into

thin plates or elongated! into ellipsaids,

The lower cross-bedded sandstone is almost identioal with the type Aldgate

Sandstone with which it has previously been correlated (Howchin, 1926).

The Lower Tremolite Rock is a thin marker hed that ean be traced inter-

tultlently on the eastern side of the Loukout Tawer Anticlne from east of

Warren Hill to the reservoir (Fig. 1), Tes surface outcrops are commonly

teplaced by massive opal, Fresh specimens consist of close-packed, interlocking,

pale preen tremolite-actinnlite crystals. On the extreme western edge of the

Wuapped arcu a finé-grained grey-blue, impure, delomitic limestone may be a

Iss metumorphosed equivalent of this bed,

The Thick Course Mica Schist Sequence erops out in a north-south helt

limediately west of the granite yneiss, and is partially replaced by the granite

gneiss. Most of these rocks have been affected by the retrograde metamorphism

STRUCTURAL GEOLOGY OF MT. CRAWFORD, S.A, 171

and the hydrothermal activity mentioned above, and bedding is almust com-

pletely destroyed, Although mineralogically simple, the rovks haye a varied

array of textures: schistose, gneissic, massive and knotted. Notable micro-

structural features are coarse grain size, strong mica orientation ses: atm the

knotted varieties), and the presence of imicro-crenulations in the schistusity.

The main mineral constituents are quartz, plaviocluse (Any 4;),. biotite, mus-

cuvite, chlorite and sericite, which in the various samples can oecur in almost

any proportion, Rarer constituents are gurmct, stturolite and sillimanite, Cuom-

run uccessories are apatite, tourmaline. haematite, magnetite, zircon, monazite,

pyrite, ilmenite and rutile. In all cases chlorite, sericite, imenite und rutile are

the secondary alteration products of biotite and aluminosilicate minerals. Plagio-

clase, of albitic compositian and with slight normal zoning, is far more

abundant in those rocks ucarer the granite enciss. Fine eryptoerystalline sericite

ocenrs either as fibrous knots after sillimanite (up to 2 em. in diameter), eom-

pact blades after kyanite (?), or us rarer hands, sometimes several inches thick,

of unknown arivin, The lattes ace concentrated most strongly in a zone uf

intense hydrothermal alteration (Fig. 1). Jn the knotted varieties feathers of

chlarite are often intermixed with the sericite. In a few specimens unaltered

fibrous sillimanite knots seem to have originated from biotite and muscuvite.

Relicts. of twisted andl Teached biotite persist among the sillimanite spindles

and account for the intermixed sericite und chlorite of the altered specimens.

Similar rephicement of mica by sillimanite has been described by Tozer (1955),

and has heen attributed te metamorphic reactions in the amphibolite facies.

Rare coarse-griined staurolite, yxumet and biotite-rich gneisses necur in the

coarse schists and are considered to have becn produced by the metamorphic

reerystallisation of rocks with appropriate composition in the amphibolite facies

wf regional mebunorphism.

The Upper Cross-bedded Arkose crops out south of (he granite gneiss

(Fig. J), and apparently lenses out northwards. It is a medium-grained quartz-

microline-wlbite arkose somewhat resembling the lower sandstone, with heavy

mineral lamination, cross-bedding and pebbles. At the granite gneiss contact

the arkose develops a gneissic appearunee and grades into the gneiss.

The Upper Tremolite Bed is a strong marker horizon outcropping with a

nfrth-south trend east of the granite gneiss. It consists af white lo pale green,

chise-packed tremolite erystals wp to several inches in length, This bed veea-

sionally carries lenses of actinolitic arkose., The tremolite rock surface oultraps

are stromyly teplaved by massive and bhoxwork opal which appears to be the

result of slow surface weathering of the tremolite, Where deep weathering has

‘ecurred the tramoalite has altered to tale.

The Pine-vruined Mica Schis! Group lies: above the upper tremolite hed

east of the granite wneiss. This unit consists of interbedded schists and thin

urkases, The schists ure much finer-gtamed than the coarse mica schists west

ol the wronite eneiss und some misht be eallecd phyllites. Thev are alsa net

affected by the extreme alteration characteristic of many of the coarser schists.

They consist of biotite, mnsecovite, quartz, albite, ubundant microline antl rare

kyanite. Some beds contuin notable arnounts of pyrite.

The Cale-silicate Group is the youngest bedrock unit in the area mapper.

Tt consists of interbedded Bne to coarse cale-silicate rocks and phyllitic finely

knotted sehists. The cale-silicate beds contiin various proportions of actinolite,

diopside, scapulite, oligoclase-andesine, quarty, clinn-zoisite, tremolite, sphene

and iron ore, Some ol the cale-silieate rocks are finely laminated while others

ah THLNST Ve anid coarse-grained,

172 KINGSLEY J. MILLS

THE GRANITE GNEISS

1. General Petrology

The granite gneiss crops ont as a single body some three miles in leveth

und np to one-third of a mile in width, The contacts of the granite gneiss ure

sharply defined; the texture of the rack being readily distinguishable from the

sumrounding metasediments, Outcrops of the pranite’ gneiss are abundant north

vf Blood and Thunder Gully (Fig, L) but south of this watercourse the vranite

weiss bonndaries can be traced only by means of strongly lateritised and

weathered floaters and residnal soils.

‘Texturally the granite gneiss grades from massive varieties poor in mice to

schistose: varieties rich in mica. A moderately strony gneissic foliation results

from preferred orientation of mica, with alternation of mica-rich lamellae with

thin (0-3 mm.) discontinnous bands jd lewses of quartz and feldspar. A

prominent lineation due to the parallelism of elongated micas is noticeable in

wll anterops. These structural features result in outcrops with a lineated bladed

form. Specimens of the granite gneiss arc almost invariably crumbly although

the grains are fresh. The freshest specimens from the watercourses are hard

and compact.

A sample of the granite gneiss was cherically analysed. The analysis, norm

wievlation and modal composition are presented in Table 1.

The mineralogical composition of the granite gneiss is variable. Vlajor

constituents are quartz, microline. albite-oligoclase, biotite and muscovite with

accessory iron ure, zircon and apatite. The quart, {20-60 p.c.) is Clear, @rano-

blastic, free of inclusions and shows undutose extinction, Quartz vrains, which

average 0-73 rmm., tend to be Jarger than the feldspar grains. Microclines, also

granublastic, show excellent tartan twinning. The microcline is always fresh

aud devoid of inelisions and constitutes 5-60 p.c. of the rock. Plaufoclase

varies from: wir accessory ti 50 pc. The composition of Any. is comparable

with that in the surrounding metasediments, Grains are equidimensional and

average 0-5 mm. in diameter, Plagioclase twinning is simple and is rare; zoning

is almost absent, Perthitic textures are absent in the feldspars although aces

sional rims of albite at plagiocluse-microclne grain boundaries may represent an

advaneed stage of easolution or the beginning of replacement. Mvimekite wud

chessboard albite appear to be absent. Biotite is the most commion mica, ayerag-

ing 2-15 p.c. Its pleochroisrn is strong from pale yellow to dark green-black

(us in the surrounding metasediments), Pleochroic haloes are common. Altera-

tion to chlorite is absent. A rarer constituent of the granite gneiss is clear.

colonrless muscovite, Lron ores. haematite and magnetite are imporlant acces-

saries ocurring in close association with the biotite and zireou. Both zircon and

apauite are impertunt accessories, the apatite occurring as small prisms im early

aud the zircons as small subrounded grains,

3. Variations in lhe Granite Cneiss.

One minor structural feature is the occurrence of a fine-grained aranite

phuse with shurp boundaries against a coarser phase. In sume cases elliptical

hichs of the finer phase up to two fect in length were observed embedded in

the coarser phase. In other cases the disposition of the coarse and finer phases

produce a pseucdo-eross-bedded appearance, Tn one outcrop two thin “veins”

STRUCTURAL GEOLOGY OF MT. CRAWFORD, S.A. 173

of the fine phase cut the coarse at a slight angle to the schistosity. Except for

less mica in the finer phase, the composition of the two phases is similar.

In places the granite gnciss has a strong arkosic appearance, with abundant

quartz, feldspar and iron ore, and lacking mica.

“pebbles” were found in the granite gnciss.

TABLE 1.

Analyses of rocks,

Several beds of sheared

Granite gneiss Amphibolite

72-85 48°67

0-38 1-66

12-73 15:05

1-29 3-12

2-13 8:70

0-04 0:17

0-63 663

1-32 11-49

2-91 2°42

4-80 +42

O15 0:26

0-46 1:59

0-07 0-09

— 9-10

49-76 100-37

Modal Compositions (Approximate)

Weight Mode Weight Mode

Quarts 39-3 a7

Plagioclase 32-0 22-2

Microcline 21-0 —

Hornbleude —_ 67+5

Biotite 6-4 _

Muscovite 0-5 a,

Tron Ore 0-8 0+5

Sphene — : 3-8

Apatite, zircon Ty 0-3

100-0 100-40

Normative compositions

Granite gneiss ' Amphibolite

Salic Femic Salic i Femic

Or 29-0 En 1:8 Or 2-5 Hy 14-2

Ab 27-0 Fs 2-0 Ab 22-5 Di 23-6

An 6-0 Ap 0-3 An 29-5 Ap 05

Q 31-3 Tl O68 | il Par

oO 0-6 Mt 14 Mt 3«3

' OL 155

93-9 6-1 54-5 45°65

174 KINGSLEY J. MILLS

4. Skialiths

A ruimber of metasedimentary inclusions, termed “skialiths” in aevordanwe

with the nomenelatuye of Goodspeed (1948), were observed in the granite

gneiss, They geocrally have a large and indefinite shape and ip all cases show

a gradational contael with the gneiss, They apparently represent tracts of schist

which have eseaped cunyersion to the granite gneiss during the granitisation

process. Their foliation ane lineation is parallel tu that in the schists outside the

granite gneiss, The major skialiths have been indicated in Fig. 1,

The skialiths show a somewhat varied mineralogy which also, however.

resembles that of the schists surrounding the granite gneiss. The skialiths are

mainly quartz-miva schists with fibroid sillimanite knots altering to seyicite.

Granitisation is induced hy the introduction of plagioclase of ulbitie compusitien

in increasing amounts. This plagioclase has a marked chessboard twin siructure

which is generally regarded as peculiar to metasomatic plagioclase, Mierocline

is ubsent in the skialiths. Staurolite is a rare constituent. Biotite schist relicts

uften have large garnet porphyroblasts, some of which reach 2 inches in diameter.

The properties of a garnet porphyroblast from a garnet-biotite skialith from the

ridge north of Baynes Gully are presented in Table 2.

4. The Contacts

Where the contacts of the granite gneiss and the metasediments are observed

parallel to the sehistosity they wre sharp, but they are gradational and inter-

tongueing where traversing the schistosity. The itertongucing ty represented

diagrammutically in Fig. 1. The castern contacts are nowhere visible and

the contacts of the southern half of the granite gneiss are obscured by deep

rick weathering and lateritisation. A thin sheet of schistose quartz-alhite-

muscovite gneiss constitutes part of the western margin of the granite eneiss.

There is a ytood schist-granite gneiss contuct un a hill 400 yards south of

the northern end of the gneiss outcrop where @ quarte-albile-biotiteemnscavite-

scricite knotted schist bas been recrystallised and a stronger schistosity developed.

Al the contact sericite knots disappear, feldspar increases in amount, microvline

appears, while muscovite is greatly reduced, With these changes the rock

develops the ynuissic texture characteristic of the granite gneiss, Just south

at this location the schists intertongue with the granite gueiss, and all gradations

vf schist to gneiss can be observed.

A number of amphibolite dykes cut the granite gneiss. These are con-

sidtved to be older than the eneiss, and thus represent sheets of basic rocks

that have resisted the granitisation, Their contacts with the granite gneiss are

shurp, although in oue case reaction had produced a hybrid rock type. This

hybrid ruck is a hornblende “granite” with hornblende, microcline, pligiovlase,

quartz, cpidote, biotite, sphene and aputite. The plawioclase is hasie (Anjo)

and strongly reverse zoned. Reverse zoning is common also in the plugioclase

al the nearby granite gneiss, Unlike the ainphibolite-granite gueiss contacts

desetibed by Chinner (1955) in the Timunda Creek area, this contact rock

does not contain diopside.

5. Alumina Metasomatism

Sillimunite-quarte pods aud kvanite peainatites of metasomatic origin over

immediately north of the granite gnciss and in the one of intense hydrothermal

alteration, bul are more commen north of the reservoir where they have been

discussed by Alderman (1942), The alumina metasomatism is belicved tv have

resulted from the expulsion of alumina-rich solutions during the granitisatiun

af originally aluntinous schists,

STRUCTURAL GEOLOGY OF MT. CRAWFORD, §.A. 5

6. Comparison with other Granite Gneisses of the Adelaide Region

Granite gneisses of a similar chitracter ocaur on @ eeeicmal scale ina NW-SE

tcending belt several miles east of the present area. ‘hese have heen stndied

in the Tanunda Creek arva by Chinner (1955) and in the Palmer area (Rathgen

Gneiss) by White (1956), Comparison of these granite gneisses with Lhe ome

inder present consideration indicates many marked similarities.

Both the Rathgen and Tanda Creek gneisses have a granitic appeardnee

with strotig foliate and lineal structural features which parullel those in the

adjacent schists. Also developed are the tollowing featwes: a slightly strained

wvinoblasti¢ texture; promincut a-c joints perpendicular to the lincation; quartz,

Foldspar, and biotite ws the major constituents: quarts showing undulose extinute

tion; plagioclase of oligoclase composition, with vare simple twinning and clear

albite rims at the contacts with microcline rrains; microcline with good tartan

twinning; general concordance und sharp contacts of the granite gneisses. with

the adjacent schists; and pre-granitisation epidiorite inclusions. All these are

features which are characteristic of the Mt. Crawford Granite Gneiss.

Both Chinner (1955) and White (1956), however, observed porpliyritic

textures, myrmekite at plavioclase-microcline boundaries, microcline replacing

Other minerals, aud alteration of the plagioclase to epidote and sericite — Features

which were not observed in the Mt, Crawford Granite Gnviss.

TILK INTRUSIVE ROOKS

1. Amphibolites

A number of metadolerite dykes, up to one mile in Tength and 100 feet

wile, have been mapped (Fig. 1), These sharply cut both the schists and

the pranite gueiss, They are fine-gramed, dark, amphiboletich schists that

have, Eirouvhout the area, 2 uniform appearance and mincral composition. They

contain dark hornblendes in parallel arrangement, zoned basic plagioclase

(Anos-a0), rarer quartz, accessory sphene, ilmenite, apatite, pyrite, magnetite

and rare garnets. In one case hornblende was seen to be altering from earlier

pyraxene. ‘These metadolerites are considered to be older than the granite

gneiss on the basis that joits in them Lave been folded during the imposition

of the younger sahistosity which is now secon in the granite gneiss, wheres

joints in the granite gneiss have vot been folded. An analysis made by the

author of w typical amphiholite, norm ealenlation and modal composition arc

presented in Table 1, Similar amphibolites have been deseribed by Chinner

(1955) from the Tanunda Creek area,

3, Major Pegmatites

Coarse-grained feldspar-rich pegmatites are common in the whole Williams-

town arent, ind extend io a belt southwards to the Gumeracha district (six

miles sonth). They generally run parallel to the north-south tectonic trend,

althuugh cross-culting peymaltes also occur. The major constituents are

plaginckise (Anois), microcline and quartz, with rarer muscovite, wnd acces-

sory beryl, tourmaline, garnet, upatite, monazite und vitcon. In places zones of

tourmalinisation border these pegmatites. According to the eviteria of Chadwick

(1958) the pegmiutites muy be considered ta be of the non-mobile, replacive

type. They show no visible tectonic orientation of their mineral constitnents,

und, because they cot both schists and the granite gneiss, they are younger than

the granite gneiss, They have heen produced on @ regional scale and have no

direet connection with the granitisation phase: that produced the granite gneiss.

176 KINGSLEY J, MILLS

TABLE 2.

Analyses of garnets

Pegmatite garnet Biotite schist garnet

f = | = =

Atums on basis Atoms on basis

Constituent, Analysis of 12 oxygens Analysis of 12 oxygens

SiO, : 36-87 2.8811, 36-96 2-948 Ly ans

Oy 0-55 0-087 f 7° 918 0-29 0.019 F2 967

Al,O, 20-48 1-896) 18-85 1-748

TiO, 0-06 0-004 + 1-957 0-27 0-016 $ 2-033

Fe,0, 0-67 0-057 J 3-14 O 260

FeO 10-68 0-701 33-68 2-246

MgO 4°54 0-531 4°82 0-573

CaO = | — 9s px 0°95 0-081 Ly ge

MnO 26-38 | «+78 7 3°989 0:75 0-051 (77976

Na,0 0-22 0-033 0-07 O-O11 |

K,0 0-43 043 0-14 0-014 J

H,0 nd. 0-08

CO,, Cl — aa

Totals 100-63 100-00

Compositions (Weight per cent)

Pegmatite garnet

Biotite schist garnet

Andradite — | 2-8

Spessartite 61-2 1-7

Almandine 24°6 7-8

Pyrope 15-1 6-0

Totals 100-9 98-3

Physical properties

| Pegmatite garnet Biotite schist garnet

| Measured | Calculated* al Measured Caleulated*

Specific gravity { 4-09 | 4-13 4°13 4-18

Refractive Index

{+ -002) 1-802 1-795 1-802 1-813

Cell Size (A) (4+ - 004) 11-599 11-573 11-517 11-533

*Based on date from Skinner (1956).

3. Minor Pegmatites

A number of small strings and veins of pegmatite, composed mainly of

subhedral microcline, quartz and accessory muscovite, beryl and tourmaline

occur in joints in the granite gneiss. The ends of these stringers appear to diffuse

into the gneiss, and are thought to represent incipient mobilisation of the rock

STRUCTURAL GEOLOCY OF MT, CRAWIORD, S.A. 177

near the end of the granitisation period. In the surrounding metasediments

pods und segrepations of pegmatilic material may be similarly mobilised matter

brought about by metamorphic differentiation.

4. Other Intrusive Rocks

Quartz veins are common in the area, especially in the zone of fitense

hydrothermal alteration (Vig. 1) where they contain considerable rutile.

MINERALOGY

Table 2 summarises the anilyses and properties of two garnets. One is a

brown spessartitic garnet from a thin beryl-tourmaline-garnet-zireon bearing

pegmatite intruded into schists west of the granite gneiss, The other is a pink,

alinandine garnet porphyroblast from i vurnet-biotite schist skialith in the

granite gneiss on a ridge north of Baynes Gully. ‘The latter garnet contained

small staurolite idioblasts which were separated before analysis, Comparison

of the measured physical propertics with those calculated from the analyses

(using Skinner's (1956) end-member data) shows apreement within the limits

af accuracy of the analyses snude by the author. Phosphorns and alkalies,

which are not usually analysed for in garnets, were found to be present in

significant amounts. Rankama and Sahama (1950, p. 587) state that phos-

phnras can replace silicon in the silicon tetrahedra. The Jigh alkali content

of the pegmatite garnet may contribute to its abnormal cell dimension.

Te was considered that a study of the relative abundances and habits of

the rarer minerals in the rocks of the arcu might help to elucidate the origin

of (he granite gneiss. Nine heavy mineral analyses were completed aud are

summarised in Table 3. The analyses show considerable variation in the relative

abundances of minerals and that there are nu assemblages peculiar to the granite

gneiss. Most of the rarcr minerals have recrystallised during the metamorphism,

except the zircon, which, in mietasediments preserves its original water-worn

characteristics, Althongh no statistical studies were made, it is clear from Fig. 3,

which compares accurate drawints of yircons from the granite gneiss, a schist

skialith, and the lower crass-bedded sandstone, that the zircons Irom the granite

gneiss are identical in size and hubit with those in the nearby metasediments.

fn contrast zircons from an igncous, intrusive granodiorite in the Cooke Hill

area (13 miles east) have a highly eubedral character. Rare rounded zircons

in the Cooke Hill granodiorite may be xenocrysts. Zircony from the major

pegmatites of the present area are of a distinctly different character from those

of the metasediments and the granite gneiss, They are waniable in size (to

3mm.), show strong corrosion, supposedly cue to alkaline solutions (Poldervaart.

1955), and have a semi-opaque, greasy, grey appearance.

STRUCTURAL CEROLOCY

Vig, 2 summarises the structural gealogy of the area. Folds in general are

overturned slightly to the west, The main anticlinal crest in the western part of

the urea (the Lookout Tower Anticline) is broken by synclinal cross-folds,

Kast of the granite gneiss the bedding S, is cut at a slight angle by a steeply

east dipping schistosity So. West of the granite gneiss the schistusity is fulded

with the development of a new foliation $., and, except in the sandstones, the

ubliteration of bedding S,. The refolding process has resulted in the develop-

KINGSLEY J. MILLS

SYMBOLS

po Bedding }

poy Foliation } vertical

vertical that

Lineation plunge

A Sedimentary faring

Trace Trace lor structural sata: 7/’

of of | tor equal area

aot serena | plata (Figure 2)! /

Structural Geology

OF PORTION OF THE

MOUNT CRAWFORD

DISTRICT

Fie. 2. Structural Geology of Portion of the Mt. Crawford District,

STRUCTURAL GEOLOGY OF MT. CRAWFORD, S.A. 179

ment of pronounced minor folds, crenulations and lineations in the schists,

Three lundred of these penetrative structures from the schists have been

measured and plotted on equal area stereograms (Fig. 4 $, D, R, W). In the

plots inhomogeneity of the linear structures is evident, but there is a tendency

for the lineations to fall on a great circle; for which there are several possible

explanations which may be summarised as follows:

A, One period of Folding

(1) Triaxial deformation (Roberts, 1960),

(2) The devclopment of Jate stage strain slip cleavages which deform an

earlier axial plane schistosity but do not intersect in the earlier fold axcs (Agron,

1960).

TABLE 3.

Heavy Mineral Analyses.

Type of Sample

Hho _ as = —- 2.2

Country

Rock. Granite. Skialiths.

K a — _ x ~ 3 —- \. —

| oA B a D iD) B G H I

Wt. Tron ore. an C | CQ vo Tr Tr Tr VC 10

in stumple. (Others astelow.| n.d, | nid, | nc Ol 05 05 | +075 2° 015

Zireon | ae A) SL 1 | 42* "47" | 33% 72 97

20 et Monazite =| 2 i 7 B7 |, BB OT 2

aras Garnet | 2 Oa | 4 | OF | Te Tr U+1

Ege sz Dyroxeno | 1-0 | 22 ‘ry | | Ty 0-1

Mees Rutile | 15 | Q-1 | 0-5 1) 10

ese Anatase | | Wl

zen Staurolite | 9 | |

PETE » Tourmaling | | ' 1 0-7 |

gees Hpidote | |

Zo Sphene | 73 ;

ae eS Graphite | | | Tr

7 Others 5) 3 | 0-5 0-8 | 2

* Invlading minor amounts of xenotime.

+ Apatite removed by acid leaching,

C—common, V¢}—very ennunon, Tr—trace, n,d.—nok dotermined,

- Hacmatite rich feldspathic sandstone: } ml. east of Warren Till.

. Altered coarse quarts-mic schist: 2 ml, north of the northern en: of the granite pneiss

outcrop,

. Granite gneiss: + ml. south of the northern end of the granite gneiss aulaurop,

iranite gneiss: Northern end of the granite grieiss outerop.

. Granite gnoiss: 13 mls. north of the southern end of the granite gnciss outerop.

. Granite gndiss: 4 ml. south of the northern end of the granile gueiss vuterop).

. Coarse quartz-mica skialith: } ml south of the northern end of the granite gneiss outcrop.

[. Haematite rich arkose skialith: 14 mls. north of the southern end of the granite gneiss

outcrop.

I. Wacmatite ri¢h arkose skialith: 3

outerop.

ml. south of the northern cnd of the granite gneiss

180 KINGSLEY J. MILLS

B. Two Periods of Folding

(1) A new foliation S, cuts previously folded bedding planes causing

lineations to lie in Sz (Weiss, 1959),

(2) Earlier lineations are rotated by similar folding (Ramsay, 1960),

The statistical data collected by the author is insufficient to decide which

of these possibilities might apply.

Fig. 3. Comparative drawing of typical zircon populations extracted fron:

1. The Mt. Crawford granite pnciss.

8. A schist skialith in the Mt. Crawford granite gueiss,

3. The lower sandstone: quarter nile west of the Met. Crawford. granite gneiss.

J. An igneous, intrusive, gneisses granmborite from the Cooke Mill region,

The granite gneiss displays a well-developed foliation and mineral lineation.

250 foliations and 200 lineations were measured in four sub-areas and are sum-

matised in Fig. 4. The attitudes of these structures are consistent throughout

the granite gneiss. Mineral lineations in the schists and amphibolites of the

area parallel the mineral lineations in the granite gneiss. These lineations were

apparently produced during or after the granitisation.

One thousand three hundred and ninety joints were measured in the granite

gneiss and are summarised in Fig. 4. The joint picture appears to vary along

the length. of the granite gneiss with a tendency for the poles of the joints at

the northern end of the gneiss to spread ou a great circle (as do the minor

folds in the adjacent schists).

STRUCTURAL GEOLOGY OF MT, CRAWFORD, S.A. 181

FOLIATION-LINEATION STEREOGRAMS,

METASEDIMFNTS

7 a

ell

‘, ao

Ss R nae Ww

‘ \

\ \

GRANITE GNEISS

JOINT STEREOGRAMS.

GRANITE GNEISS

ig. 4. Equal area projections of the poles of structure elements measured in the

granite gneiss and surrounding metasediments. ‘The letters refer to the corresponding sub-

areus marked on Fig, 2,

Folfution-Lineation Stereograms

Metaseciments

S 18 lineations measured in Watts Gully, ‘

D 1S foliations and 90 lincations (contoured at 1, 2, 4, 8 and 12 p.e.) measured on «i

single schist outcrop aboye the dam in Dam Gully.

K 100 lincations (contoured at 1, 2, 3, 5 and 10 p.c,) measured. in the schists immediately

north of the granite gneiss.

W 26 foliations and LOO lineations (contoured at 1, 5, 10, 20 andl 30 pic.) measured al

the South Warren Reservoir weir.

Granite Gneiss

a LOL foliations andl 95 lineations (both contoured at 1, 5, 10, LS and 20 pc.) measured

in sub-arca G,,

G,, 74 foliations (contoured at 1, 5, 10, 15 and 20 pyc.) and 37 lineations measured in

sub-area. Gy.

+, 45 foliations and 41 lincations measured in sub-area G.,

CG, 31 foliations and 25 lineations measured in sub-area Gy.

Joint Stereograms

Granite Gneiss

G, 264 joints (contoured at 1, 2, 3, 4 and 6 p.c.) measured in sub-area G,.

+, 380 joints (contoured at 1, 2, 3, 6 and LO p.c.) measured in snb-area G,..

G, 446 joints (contoured at 1, 2, 4, 6 and 10 p.c.) rneasured in sub-area G,.

Gy 300 joints (contoured at 1, 2, 3, 5 and 10 pic.) measured in sub-area Gy.

1§2 KINGSLEY J. MULLS

CONCLUSIONS

Lvidences in fayour of granitisation are: the complete lack of ignecs

loxtures or structures in the granite gneiss, lack uf evidenee near the granite

gneiss for mechanical croplacement and wide variations in the relative abnnd-

ances of both the major and the minor minerals in the gneiss. There are,

however, no visible acid igneous rocks in the area to which the causes of grani-

tisation might be ascribed,

The granite gneiss is concluded to be of metasomatic origin. “The strongest

direct evidence in support of this is gained from a comparison of zircons from

the sediments with those from the granite gneiss. Polderyaart (1950) advocated

the use of zireons as a eriterion of the granitisation of sediments. Fander

(1961), working on some local South Australian granites, showed that m most

cases the origin of a granito could be indicated through zircon studies. During

metamorphism zircons do unt ceerystallise until the highest grades are reached

(Polderyaart and Backstruin, 1949). Zircons in igneous granites are almost

invariably euhedral, rare rounded oes probably being xenoerysts. In the

Mount Crawford Granite Gneiss none of the zireons are perfectly euliedral and

there is a predominance: of rounded types. Zircons in the granite gnetss are

identical with those in the metusediments.

The chemical changes that oecurred during the granitisation cannot be

assessed without further chemical analyses, However, it is believed that only

minor chemical changes would be necessary to convert the schist to granite

gneiss, The major factor causing the wranitisation was probably a change in

water vapour pressure. Within the granite gneiss this would result in a new

mineralogical equilibrium whieh apparently involyed a reduction of the amenunt

of mica (especially muscovite), and an increase in feldspar (especially micro-

cline), Lower water vapour pressure and temperature outside what is now the

uranite gneiss resulted in a zone of retrograde and hydrothermal alteration in the

schists surrounding the granilised core. The sillimanite-quartz pods and the

kvanite pegmatites in this yone may have been produced by the expulsion of

some of the alumina and silica from the originally aluminous sehists during the

“ranitisution. Late stage reerystallisation of the granite gneiss has almost

obliterated replacement textures which might have more clearly indicated the

vranitisation process,

Similar granitic eneisses ta the east have been considered to have a grani-

tived origin, Chinoner (1955) regarded the Tanunda Creek granite gneisses as

recrystallised schists with a slight addition of alkalies. White (1956) proposed

fut a slight expulsiow of silica was all that was necessary to convert original

mictasediinents into the Rathgen granitic gneiss,

ACKNOWLEDGMENTS

Expenses in connection with this work were defrayed by the University of

Adwlaide Research Grant. The writer wishes to acknowledge gratefully the

het atl advice and encouragement given by the Geology Department staff and

eolleagnes. The assistance of Dr. KR. L, Oliver and Dr. J. L, Talbot of the

Ceology Department in reading and criticising the manuscript is greatly appre-

ciated,

STRUCTURAL GEOLOGY OF MT. CRAWFORD, 5.4, 183

REFERENCES

Aguon, S. L., 1930. Structure and Petrology of the Peach Bottom Slate, Pennsylyania and

Maryland and its environment. Geol, Soc. Amer. Bull., 61, pp. 1265-1306.

Aungnman, A. H., 1942. Sillimanite. Kyanite and Clay Deposits near Williamstown, South

Australia. Trans, Roy, Soe, S, Aust. 66 (1)

Campana, B., 1953. Ceological atlas of South Australia, Sheet Gawler, Geol. Surv. S. Aust.

Campana, B., 1955. The structure of the Eastern South Australian Ranges; The Mt. Lofty-

Olary Are. Journ, Geol, Soc. Aust, 2, pp. 17-62.

Casmana, B., and Wuirrus, A. W. G, 1953, Lhe geology of the Gawler Military Sheet.

Report of Investigations 4. Geol, Sirv. $. Amst.

Crapwick, RK. A. 1958. Mechanisms of Pegmatite emplacement. Geol. Soc, Amer. Bull.,

69 (2), pp. 503-836,

Cuevnun, G. A., 1955. The granite gneisses af the Barossa Ranges. M.Sc. Thesis, University

of Adelaide, Unpublished.

Fannen, H. W., 1961. Accessory minerals of South Australian granites, M.Se. Thesis.

University of Adelaide, Unpublished.

Goonserrp, G. E., 1948. Xenoliths and skialiths, Amer. Journ. Sci, 246, pp. 515-525.

Hovrexp, P.-$., 1935. he geology of part of the Northern Mt, Lofty Ranges. Trans, Roy.

Soc, S, Aust., 59, pp, 16-67.

Hower, W., 1926. ‘The geology of the Barossa Ranges and neighbourhood in relation

ty the geological axis of the country. Trans, Rey, Soc. S. Aust. 1, pp. 1-16.

Mosc, BP. 1949, Metasomutic aranitisution of athiylithie dimensions. Amer. Journ. Sei.

247, pp. 209-245, 372-406, 673-705,

Porpervaant, A., 1950. Statistical studies of wircon as a criterion of granitisatiom. Nuture-

165, pp. 574-575.

Pornmnvaanr, A. 1935. Zircons in rocks. Amer. Journ. Sei, pp. 433-461,

Potprnvaant, A. and Bacxsrrdat, J. W,, 1949, A study ofan area at Kakamas (Cape Pro-

vince). Trans. Geol. Soe, S. Africa, 52 (1), pp. 483-495.

Ramsay, J. G.. 1960, The deformation of early linear structures in area of repented folding.

Journ, Geol, 68, pp. 75-93.

Ranxama, K., and Samama, Tu. G., 1950, Geoeheristry, Uniy. af Chicago Press.

Rozexts, J, L., 1959. Fold structures in Dalradian rocks of Knapdale, Argyllshire. Geol,

Mas., 96 (3), pp-

Ssinner, B, J., 1956. Physical properties of end members of the garnet vroup. Amer. Min,

41, pp. 426-436,

‘Yozrr, G. F,, 1935. The mode of occurence of sillimanite in the Clen District. Co. Donegal

Ceol. Mag., 92, pp. 310-324),

Weiss, L. F., 1959, Structural analysis of the basement systend at 'Turoka, Kenya. Overseas

Geology and Mineral Resources, 7, pp. 3-35 end 123-163.

Wane, A. J. B, 1956. ‘The eranite gneisses and associated metamorphiy rocks of Pahner.

South Australia. Ph.D. Thesis, University af London, Unpublished.

Woonwann, H, 2, 1886, Notes of gealogical map of Gumeracha and Mt. Crawford Gold-

fields. Duper 62, Parl. Iipers of 8. Aust., 1886.

RETROGRADE METAMORPHISM OF THE HOUGHTON COMPLEX,

SOUTH AUSTRALIA

BY J. L. TALBOT

Summary

Rocks of the Houghton Complex (?Archaean) have undergone at least three periods of

metamorphism. The earliest period, as deduced by relic minerals, was at the upper amphibolite

facies. The two successive periods of metamorphism were at the lower greenschist facies. Studies of

the overlying Torrens Group rocks (Upper Precambrian) suggest that these last two periods of

metamorphism occurred before and after the deposition of the Torrens Group respectively.

RETROGRADE METAMORPHISM OF THE HOUGHTON COMPLEX,

SOUTIT AUSTRALIA

by J. L. Tavsor*

[Read 9 May 1963]

SUMMARY

Rocks of the Houghton Complex (PAretiacan) have undergone at least three

periods of metamorphism, The earliest. period, us deduced by rclie mimerals,

was at the upper amphibolite facies. The two successive periods of meltamor-

phism were at the lower greenschist facies, Studies of the overlying Torrens

Group rocks (Upper Precambrian) suggest that these last two periods of mnta-

morphism occurred before and after the deposition of the Torrens Group

respectively,

INTRODUCTION

Rocks of supposed Archaean age are present in several areas of the Mt,

Lofty Ranges. Disconnected masses, separated by a cover of Permian, occur

between Mt. Compass and Yankalilla (Fig. 1), Other inliers, surrounded by

younger Precambrian, occur in the neighbourhood of Aldgate and in the vicinity

of Houghton, It has long been recognized that these inliers show similar

petrographic features and appear to have undergone similar mclamorphic

histories (Benson, 1909; England, 1935). Benson (1909) recorded that many

of the high-grade rocks in the inlier around Iloughton show signs of alteration,

and this alteration has been discussed in more detail by Alderman (1938) and

Spry (1951). Alderman concluded that the alteration was the result of dynamic

metamorphism subsequent on a higher grade phase of metamorphism, Spry

correlated this alteration with the deformation of the overlying upper Pre-

eambrian rocks.

lt is the purpose of this pauper to describe the various retrogressive changes

which have affected the rocks in one of the inliers (the Houghton Complex)

and to relate these changes to the overall metamorphic and structural history

of that part of the Mt. Lofty Ranges. It is only after a study of the effects of

the retrograde metamorphism that the nature of the original rocks can be pro-

perly discussed.

* Geology Departinent, University of Adelaide.

+ The term Houghton Complex is used to describe the complex of metamorphic rocks

which Howebin (1926) termed Houghtonian, ‘his change in name is in accordance with

the Australian Code of Stratigraphic Nomenclature (Anon,, 1958, Article 31). The racks

which surround the Hoaghton Complex are part of the Torrens Group of Upper Precambrian

age (Daily, 1963, discusses the nomenclature of these younger rocks),

Trans, Boy, Soc, §, Aust, (1963), Vol, 87.

186 J. L. TALBOT

Cainozoic N

Permian

Cambrian

, ADELAIDE

U.Precambrian a

“archaean”

COlder Precambrian) .

7’ wlagate - - 1 -

“Mt

Kompirs el

ENCOUNTER BAY

Fig, 1.

RETROGRADE METAMORPHISM, WOUGITON COMPLEX, 8.4. 1&7

THE PETROGRAPHY OF THI RETROGRADE ROCKS

‘The original higher grade rocks of the Houghton Complex appear to have

beer quite yaelable in chemical and mineralogical composition, ni the region

aronnd Loughton and around Kersbrook (Fig. 2) are large masses of rock

vomposed essentially of feldspar with minor amounts of amphibole und diopsidic

pyroxene, In other parts of the complex, rocks meher in quartz are common

and were probably quartzo-feldspathic schists and gneisses. The rocks rich in

feldspar show alteration different from the other rocks of the complex, und these

changes ure described separately. It is realised that the differences behween

styles of alteration may reflect differences either in degree or type of alteratiun,

in original composition or combinations of these effects,

Alteration of the leldspar-rich Recks of Houghton and Kersbrook,

The feldspar-vich rock types (divrites of Benson (1909): metasuimuatisedt

sediments of Spry (1951) ) show a greater number of relic features than do other

racks in the complex and the present outerops of feldspar gneisses proliuhly

represent the least altered rocks in the complex.

Mineralogically, the feldspar gneisses consist o£ plagioclase and mivracline

in varving proportions, with minor amounts of amphibale and dinpsidie pyroxene.

Plasiovlase, whose cofmposition ranges from An, to Any is the aore

abundant feldspar. Perthitie relationships arc common and mictocline fs

dominantly a fine vein perthite. Antiperthiles and irregalar patel: perthites alsu

we common, The feldspars show differential alteration; the microcline shows

less signs of alteration than the plagioclase, Even in rocks where the plagioclase

is almost completely altered, microcline is commonly unaltered, In fine film

perthites the albite lamellae show alteration although the host microclines ure

wnaflected. Plagioclase shows two types of alteration. A dusty alteration to

epidote resembles the normal saussuritization, The altered plagioclase slows

no vuriation in composition within a single grain, although in diflerent speci-

mens the composition may range from Ari toa Any.

Sericite is another common alteration product of plagioclase and its develap-

ment appears lo be quite distinet from the: alteration to epidote. The sericite

wrains are commonly randomly distributed throughout the plagioclase grains,

hi most cases the sericite shows no obvious ortentation relationship to the plagio-

vlase, but in some specimens the flakes lie in the {001} cleavage plane of the

plasiuelase and less commonly in the (010) cleavage and twin boundary planes,

tn many specimens the sericitic alteration is patchy and the sericite may he

concentrated in grain boundaries, ar eross fractures or in irregular patches

within single gains, In some grains the alteration may be so advaneed that

the nature Of the original prain is hardly discernible. In contrast with the

saussuritization, (he alteralion to sericite results in variations in the composition

of the plagioclase within individual grains. Those parts of the grain which

show parebes of ahnnrlant sericite are more ulbitic than the portions relatively

free of sericite.

Pyroxene always shows more or k¢ess complete alteration to actinolite. In

some specimens needles of actinolite project from large diopside grains inte

the surrounding feldspars, but more commoriy the horders of the pyroxenes are

completely altered or the actinolite may vccur in patches within the pyroxene.

Actinolite, however, is not restricted to an association with pyroxene. Some

specimens contain large discrete grains of actinolite rather than bundles af

188 J. L. TALBOT

needles, Actinolite muy also be concentrated in fractures and small faults. It

appears that there has fee considerable mobility of the actinolite constituents.

It is not known whether any of the large discrete amphibole grains were original

constituents of the higher grade rocks.

Epidote is another minera] characteristic of the retrograde metamorphism

of the feldspar gneisses, Commonly it occurs as very small granules or dust

- a MT.GAWLER ---. f

b GIIE a,

ef foe)

H , yor HL BROOK

', HOUGHTON “ey 2, | 2RESERVOIR

eye Vike,

ryt

TORRENS GROUP

Quartzite

EY Dolomite

Phyllite

HOUGHTON COMPLEX

Feldspar gneiss

Qtz-feldspar gneiss

Mica gneiss

Ei] Blastemylanite

Fig, 2. Sketch geulogical map of southern part of the Houghton Coniplex.

RETROGRADE METAMORPHISM, HOUGHTON COMPLEX, S.A. 15u

enelosed in the plagioclase grains and presumably is a product of saussuritiza-

lion, In other specimens the epidote occurs in clusters of larger grains. also

enclosed in plagioclase, or as interstitial grains. Epidote is also commun in

some layers rich in actinolite, in which layers its concentration uppears to he

tio great to have been derived from Teldspar. Epidote also shows considerable

mobility ane oceurs in Jinge patches and in veins which cut across bath feldspar

and actinulite.

Brown biutite is a rare constituent of the feldspar gneisses and where

present is commonly altered to an olive-green variety with rutile needles ar-

ranged in a hexigomid network in the basal plane, ‘The biotite allernatively is

crowded with granular opaque minerats.

Associated with the chemical changes numerous signs of deformation are

observed ia the fellspar gneisses, Quartz, where present, invariably sheaws

nndulose extinction or strain bands. Microcline commonly shows undulose

extinction, and plaginglase twine lamellae are kinked in some instances. Recorys-

tallization oF plagioclase to fine-grained anhiedral aggregates is rarc. Mast

commonly finerprained uggregates culling plagioclase erains are composed ot

quarty (and. sericite). A few specimens show course-grained aggregates of

playioclase and actinolite; hese textures may be the result of recrystallizatinn.

The plagioclases in the Kersbrook feldspar gneisses show a texture which is

commonly called chequer-alhite (Gilluly, 1933; Starkey, 1959) (Fig. 1). The

albite-law twins are short and alternate along their length giving a chequer

heanl appearance to the prains (18251, 18252),% Although this texture has

heen considered to be the result of metasomatie replacement of potash feldspar

(Gilhily, 1933), it is now commonly thought to be the resalt of some reerystal-

lization process (Battey, 1955). Starkey (1059) showed that the development

uf chequer-albite in porphyries from New Brunswick was correlated with

increasing deformation, Certainly a deformation origin would better explain

the Houghton Complex occurrences. Replacement (or redistribntion) texteres

in the feldspars of the Tloughton Complex are characterized by irregular vein

or patch perthite,

Alteration of Quartz-Feldspar-M ica Cneisses

Schists and gneisses rich in quartz and feldspar occur to the west of the

feklspar gneisses at Houghton and in portions of the Torrens Gorge near the

western border of the complex. ‘The gneisses are characterized by good cum-

positional layering; the Houghton examples were originally mapped as part

of the overlying Torrens Group (Sprigg et al, 1951), although they were later

recognized as part of the older Honghten Complex (Spry, 1951). The ean-

fuxian acose because of their apparently bedded appearance (excellent examples

can be seen at the entrance to Houghton School, Grid ref, 757-064). The layer-

ing appears in hand specimen to be dne to alternations of quartzo-leldspathic

material with layers rich in phylosilicates, Jn thin section the apparently smica-

geous layers are secn to be zones of greater alteration. The altered zones

consist of a fine-grained quartz-sericitet ayyregate enclosing rare relics of quartz,

microcline, coarsé mica and rarer plagivelase. The oricntation of the layers is

parallel to the preferred orientation of the coarse relic muscovite in the unaltered

* Specimen numbers refer to specimens on file i Lhe Ceology Department of the

University of Adelaide,

_ } Sericite is an informal term used here for fine-grained white oticu. ‘Mie mica is a

2M museayite,

190 J. L. TALBOT

layers. The altered layers vary: in thickness up to about 3 ram. The relatively

unaltered layers vary up to a few centimetres thick, The origin of the alteration

or its contol is not fully understood. It is possible that the alteration took

place in zones which are tectonicully controlled (e.g. closely spaced shear

zones). Alternatively the alteration may have been selective in layers which

differed compositionally from the unaltered lavers, These two hypotheses

cannot be distinguished on the evidence available.

Binstomylon'tes and Phylloniles

Over much of the complex the devree of ulleration is so great (hat original

textures and structurcs have been to a large extent obliterated, and the rocks

have suffered more or Jess complete recrystallization and neomineralization.4

Many of the rocks are classified as blastomylonites, a term used by Sander (sve

Christie, 1960) to cover all “cataclastivally” deformed rocks which have heen

recrystallized (or neomincralized), Some of the rocks are phylonites (Knopf,

1931) which are retrowrade rocks resembling plyilites but haying an origin

similar to blastomylonites. Phylonites are characterized by a micruangen

siruintare.

In hand specimen the rocks vary greatly in appearance. In the less altered

quartzo-feldspathie gneisses, a goad secondary foliation ts well developed, am-

roonly parallel to the gneissic layering but in other occurrences at a distinet

angle to this laveriny, With more advanved alteration the foliation develops

intu well-defined layering and the resulting rocks resemble the flaser vuvisses

deseribed hy Hainiltow (1960). The layering varies fram 1-10 cm. in thickness

separated by thinner serteitie zones. In some outerops the individual layers are

unilorm and are persistent over severu) metres; in others, the less altered portions

are lensoid and irregular. With further alteration the rocks are poorly layered

and possess only av foliation which is a penetrative structure affecting the whole

body of rock.

Many of the rocks show augey structure. Alderman (1938) has described

the angen gneisses north of the area mapped by the author, The augen are

large (up to 3 am, wide) and are composed of individual feldspar grains com-

niwuly larger than Lem. in size. Alderman, in a study of the chemistry and

mincralowy of the augen gneisses, concluded that the anven originated by growth

at the quartz and feldspar due to metasomatism. Larlicr, Hossfeld (1935)

concluded that the wugen were crnshed pegmatitie and granitic material. Spry

(1951) demonstrated that the development of the schistosity associated with

the augen gneisses is Inter than the crystallization of the angen material and

vanvluded that the schists were not the source rocks of the sugen gneisses

dnd that the processes were more complex than that envisaged by Alderman.

The ultimate origin of the Humbug Serub gneisses can only be partly

deduced owing ta the widespread sericitization, but the grait size of the quartz

ancl feldspars is large compared with the normal grain size of high-grade rocks

in the Houghton Complex. Processes involving either peymutitization or muta

sumuttisn( are reasonable origins for the particular high-grade rocks of that

area. The Humbue Serub yrcisses show similarities to those seen farther south,

aie this author would agree with Mussfeld thut the development ot the amen

is lurgely determined by subsequent retrograde changes, In the area exqmined

+ Neominereligition is au tet used for erystallizahion amder metamorphic eonditions in

whieh new minerals are formed (Kopf, 1937),

RETROGRADE METAMORPHISM, HOUGHTON COMPLEX, 5.4, 191

by the author the large augen characteristic of the Humbug Scrub region are

rae. Smaller augen, commonly 1 em, wide, are more common, although

examples comparable in size with the Humbug Serub xugen are found in the

Torrens Gorge. Howeves, the duternal stvucture of the augen differs tron those

deserihed by Alderman. Large subhedral grains of feldspar are rare and the

agen are composed of an agyrogate of fmé-wramed gqnartz with strained relies

ol quartz, microcline and rarer albite. Vhe rocks in which the augen are found

are commonly layered with the augen furming prominences in individual Juyers,

The cocks resemble augen schists (Lapwerth, 1885) which are common in

areas characterized by mylonites. The differences between tle augen in the

River Torrens area and thase of Humbug Scrub are considered to be due to the

groatcr degree of alteration and reerystallization in the southern part of the

cumple,

Two distinet textural types were produced during the alteration; one type fs

characterized by no distortion of the relic minerals and no preferred orientatiun

al tetragrade minerals; the other type shows evidence of considerable strain,

ln the first type alteration has oeeurred leaving the shape of the original mineral

undistarbed. In this category is the alteration of feldspars to sericite with no

preferred orientation of the sericile. Similarly perfect cross sections of silli-

muanite are preserved as a mass of non-oriented sericite, and presumably irregular

patches of sericite represent this sare type of complete replacement, The end

wodiuct of this alteration is a rock with relics of quartz and microcline in a

inewrained quartz-serleile ugeregate (Fig. 2). Kubedral tourmaline and

magnetite are also found in the fine-grained aggregates and are considered tu he

late stase minerals. In the second type, the alteration tends to he concentrated

in distinct sub-parallcl zones and within these zones the sericite shuws a strang

pruterred urientation, and relics are relatively uncommon. With an increase

in’ the number of zones the rocks heeorme schistose and many show the typical

uugen structure, The relic minerals, which im the early slages of altevation

show no shape preterred orientation, in the later stages lave their long axes

aligned parallel to the sericitic foltution,

Th extreme examples of alteration and deformation rocks resembling plillites

or rooling slates are observed (18243, 18246) (phyllonites of Knopf, 193h. see

also Spry, 1951). In thin section they appear as finely laminated slaty rucks

with an average urain size of less than -005 mm, with relic elongate lenticular

quarlz uveroyates of somewhat larger grain size (-01 mm.). Zones of true

phyVoniles are not comman in the large area of blastamvlouites ancl tweur

mainly as Uhin zones cutting the massive feldspar gneisses.

Commonly the oriented sericite zones cnt across the areas of non-oriented

patches ol quartz-sericite suggesting thet the orientation process is later than

much of the alteration. Whether these elfoots are the result of two phases ol!

alteration ur parts of the same phuse is nol known.

Assuciuted with the retrograde chanyes is a considerable degree ot defarma-

tion of the relie minerals, Although deformation effeels are visible even in

rolatively unaltered rocks, they are most apparent in the foliated sevicitearich

rocks, Quartz shows a greater variety of deformation features than the other

minerals and exhibits undulatory extinetions, strain bands, fracturing, marginal

erinulition and reerystallization. The extinction bands are parallel to the

LOQ0!] axes of quartz (eg. Hietanen, 1938). The fractures are irregular and

show no tendency to oeeur parullel tu the extinetion bands as reported by Bailey

and athers (1958),

192 ]. L. TALBOT

Many of the large quartz grains have recrystallized to a mosaic of small

unstrained grains (commonly ca. -01 mm.). The small grains are commonly

polygonal in outline and tend to meet in triple points (Voll, 1960), Where

sericite is present in the aggregate the grain boundaries are modified and

quartz-quartz, interfaces tend to lie perpendicular ta sericite {001} planes,

The distribution of small quartz grains is not constaut. Some large grains

show sutured boundaries which are commonly due to a single layer of inter-

granular polygonal grains whose orientations are closely related to the adjoining

large grains (Plate I, Fig, 3). In a few examples, stringers of polygonal grains

cross single large grains of quartz (Plate 1, Fig. 4), the recrystallized grains

having an orientation similar to the host grain (Tig. 3),

Fig. 3. Quarlz orientation diagram of sinall grains en-

closed in 2 single large weain, The average orientation

of the Jarye strained grain is shown as A. Spee. 157-172

220 grains, Contours 1-2-3-4 pc. per 1 pie. area.

More commonly the recrystallized quartz grains occur in aggregates and

in many cases guly relics of the large grains remain enclosed in a polygonal

aggregate of quartz and sericite. In other cases the polygonal grains occur as

tails on the larger, straincd quartz grains.

The textural features described above are interpreted as changes brought

about by deformation. Undulatory extinction and extinction bands in quartz

haye been interpreted by Bailey and others (1958) as polygonization effects

resultant on detormation by bend gliding. The widespread development of

fine-grained polygonal quartz ty interpreted as recrystallization and grain growth

from a stressed aggregate, the relics of which are still visible (Voll, 1960; Griggs

and Handin, 1960), In quartz-sericite aggregates the textures sugvest contem-

poranicous yeerystallization of these minerals and possibly the widespread

sericitization is contemporaneous with tho recrystallization, This suggestion is

supported by the generally preater degree of sericitization in the more deformed

aggregates,

Structures Associated. with the Retrogressice Metamorphism

As noted previously, the most common structure associuted with the retro-

grade metamorphism is the foliation. Commonly, in the Jless-altered gneisses

in the River Torrens region, the foliation is parallel to and accentuates what

may have been original composition layering and where this layering is folded

on a Jarge scale, the foliation is also folded. However, in the more altered parts

of the complex the foliation and associated metamorphic Jayering is not

RETROGRADE METAMORPHISM, LOUGHTON COMPLEX, 8.4, 193

pasallel to the cumpositional layering but forms a distinet layering whieh is

parallel to the asial surlace of small folds in the original layering. It fs nat

possible to recognize clearly any pre-relyogvade structures iw the schists and

encisses and even broad folds in the feldspar gneisses have axes whieh lie in

the retrograde foliation, ‘The only structure whiel can be determined with

corti to be piterelragession is the layering in the feldspar ynpisses.

TUR METAMORPIISM OF TILE UPPER PRECAMBRIAN SEQUENCE

(TORRENS GROUP)

In order to discuss the relationship of the retrogressive metamorphism ts

the overall metamorphic history of the area a short statement of the more

important aspects OF the metamorphism of the Torrens Group is viven here.

The Towrens Group, which Mawson and Sprigz (1950) called the Torren-

sian Series, consists essentially of a sequence of phyllites with prominent quartzite

horizons (e.g. Slonyfell Quartzite) and dolomite horizons (ew. Citstiumbul,

Montacnte and Beatimont Dolomites). Minor quurtzites and dolumites oecur

in additiog throughout the sequence. In certain parts of the area basal con-

slamerates and haemitite-rich quartzites rest on the rocks of the Houghton

Complex, However, the relationship of the conglutaerites to the overlying beds

is unknown sitice faulting is widespread on the west side of the Houghton

Complex and the outerops are poor along the south and cust of the complex.

The conglomerates contain pebblos which can commonly be matched with

the udjucent Ifonghton Complex rock types. In the region of Houehton

pebbles of a varicly of feldspar and quartz feldspar gneisses are abundant

(18249, Grid ref, 763-975). By comparison the conglomerate outcrops just

north of the River Torrens (18248) contains much more quartz and retrograde

gneiss, reflecting the more highly altered character of the Houghton Complex

ju that vicinity. Pebbles of retrograde gneisses and schists also are conimon

in the conglomerates wong the eastern margin of the complex.

The retrograde chauges are thought to be pre-depositional, since the degree

of alteration varies considerably from one pebble to unother, much more than

lhe variation in alteration observed on the same scale in the Moughton Complex.

Some pebbles show retrovrade effects which are as great as those in the

Houghton Complex, and therefore it is concluded that much of the retrugrade

metamorphism affecting the Wougliton Coraplex occurred before the deposition

af the Torrens Group conglomerates.

The metamorphisin of the Turrens Croup appears to be of lower green-

schist facios, The phyllites consist of quartz, sericite, chlorite and minor feldspar,

and in some cases considerable carbonate is present, ‘lhe sericite and chlorite

show a distinct preferred orientation and impart a good cleavage to rocks rich

in those minerals. Other rock types contain few indicatary of metamerphic

arade, Many of the quartzites stl show evidence of the clastic nuture uf the

srains although most of the grains are strained. Strain shadows pass through

grain boundaries into the adjacent siliceous cement; thus the straining is al

least partly induced by post-depositional deformation, In contrast with the

Houghtou Complex, reervstallization of the large quartz grains to a fine-grained

polygonal ageregate is nat very common or so complete. However, mylonile

rocks are found in various places (Crouch’s Hilf and east of Mt, Gould, 18253)

and in these occurrences the quartz occurs in layers of fine-grained individuals,

vaeh layer showing a marked preferred orientation, which is different from

that of adjacent layers,

194 J. L. TALBOT

The dolomites ave completely recrystallized, and the clastic quartz grains

enclosed in them are commonly deformed, Microcline grains arc subrounded

ta roonded und show authigenic microcline outgrowths similar to those deserihed

hy Baskin (1956). The quartz grams, on the other hand, are commonly Leoti-

cular and higlily strained and are elongate parallel to the Jocal foliation where

present. In some Specimens (18245) the quartz has completely recrystallized

with the dolomite.

THE METAMORPHIC HISTORY OF THE HOUGHTON COMPILES

It has Jong been revoynized that the Torreus Group rocks ia the eegion of

the Houghton Complex are of a comparatively low grade uf metamorphism,

Kiueks of a higher erade of metamorphism occur a few miles to the east of the

Hraghtom Complex; assemblages contain undalusite, staurolile, kyanite, garnel

and sillimanite (Kleeman and Skimmer, 1958). Woolneugh (1908) conchided

these high-erade rocks were Archacau and called then the Burossian Compiles.

tlowever, it is now clear thet fhese rocks are Cambrian or vonnger in age (see

wg, Campana, 1958) and that the metamorphic zoning in the Mt Lofty Ranges

is quite independent of the ontcvops of the older rovks (Kleeman and White.

1956).

The Houghton Complex ovcurs ina zone of metamorphism where the sur-

rounding Torrens Group is at the lower greenschist ficies, The present meta:

nunphie grade of the Houghton Complex is consistent with this grado. However.

it is believed that the older rocks were essentially at this grade before the

deposition of the Torrens Group, Evidence for this (as detailed previously) 1s

wontaived iu the pebbles of the basal conglomerates.

The Toughton Complex therefore appears to have suffered fvo phases ol

metamorplisin wt the greensehist facies, although no direct evidence for this is

deteotable in the complex itself. Spry (1931) caneluced thet the foliation m

the Lloughton Complex. and Torrens Group racks were produced at the same

hime. Evidenee for this is limited to the demonstrably secondary natiye ot tie

foliation in the Houghton Complex and the parallelism of the foliations in both

protps of rocks. "This parallelism, however, could be due to the continuity of

the sume system of stresses over u long pertod (or successive periods) of time.

Evidences lor earlier phases of higher grade metamorphisin in the Mousliton

Complex is rather limited by the later rewowrade changes. The racks have a

high-urade aspect, and suites which can be recognised ag injection pneisses

ar inctasomatized gueisses have long been reported (Towchin, 1906, Alderman.

1938). Of more problematical origin ure the feldspar gneisses (diarites ut

Bengon, 1909; wranulites or melasomatized sediments of Spry, 1851). As far

ag ean be determined, the feldspar cnueisses were originally composed of an

weeregate of plagioclase of oligoclase to andesine composition (Atta a5 ce the

mast caléic plagioclases observed as relics), with minor amounts vt diepsidic

pyrexene and possibly same horublende, Mievocliie 38 common in sding af the

feldspar gneisses apd is most commonly perthitic.

QOnartzrich gneisses alsoare common in the area around Loughton and the

Torrens Gorge. Thiese giieisses ave quite distinet from the appar gnuisses in

nutcrop. They appear to have consisted of quartz, feldspars and micas, and in

some of therm the quartz grains are in fattened spindles characteristic af grann-

litic Fabric. Silliminite, andalusite and gamet occur sporadically as relics

throughout the complex, The mineralogy of the feldspar gneisses and the uther

relic rock types in the complex are consistent with an upper amphibolite tucies

of suelamearphism (Fyfe ane others, 1958),

RETROGRADE METAMORPHISM, HOUGIITON COMPLEX, $.A, 195

In some parts of the complex the structure and inmeralogy of the original

rocks is still readily discernible, However, throughout most of the complex the

nature of the pre-retrograde rucks is in some douht. Ut is elear that the rocks

musl have been a variety of Jigh-grade. schists and gneisses, but their inineralogy

and fabric haye been largely changed hy retrogression. Attempts to evaluate

any changes which must have taken place to produce the feldspar-rich rocks

from the “normal” schists (Alderman, 1938: Spry, 1951; Webb, 1953) are open

to the objection that the original composition of the schists is unknown, The

greater feldspar and Na.O content of the feldspar gneisses may reflect merely

the destruction of feldspar in the retrograde rocks and the simultunecs removal

of Na..O from these rocks. However, the felelspar gneisses. which may contain 100

pc. feldspar, must have heen distinet rock types as no type of retrograde

change observed in the complex could result in the common rocks with coarse-

ernincd quarts relics.

[tis concluded that the original complex consisted of racks of the upper

smphibolite facies, consisting of feldspar-diopside gneisses and a variety of

quarty-hearing schists and gneisses. These rocks underwent two phases af

relragressive metamorphism to produce the sericite-rich blastomylonites aned

auugen guvisses characteristic of most of the complex. The feldspar gneisses

appear to lave been mere massive and have resisted the retrogressive changes

to @ greater extent than the other rocks of the complex.

ACKNOWLEDGMENTS

The author wishes to acknowledge the advice and assistance of bis el

leaves in the Geology Department at the University of Adelaide, Drs, TR. L.

Oliver and A. W. Klceman kindly read and criticised the manuseript.

The anthor is indebted to the University of Adclaide Research Fund [or

defraying expenses ineurred. im field work.

REPEREN CES

Annrnaray, A, RB, T1938. Auge arisses in He Humbuc Scrub area, Sonth Australian, Means.

Ray. Sou. 5. Aust, 62. yp. LGS-LOl.

Aspoanions, 1848. Anstralion Code of Stratigraphic Nomenclature (third érlition)d, Jour,

Geol Soe. Anst, 8. pp. 63-70,

Baitey, S$. W,, Bec, R.A. aml Pose. C. f., 1955, Plastic deformation af quarlg in wabure-

Bull, Geol Soc. Amer, 69, pp. 1143-1466.

Basery, Y., 1956, The stedy of anthigenic feldspar. Jour. Geol. 64 p. 132,

Barrey, M, FH. 1955. Aikuli nmclasouatisur and ie petcolowy of sane keratophyres. Ceol,

May. 92, pp. 104-126.

Venson, WiN. HIOG. Peteographical notes on certain Preauobria rocks of the Mt Letty:

Ranges with special reference to the geolegs of the Tloughton district. Trans, Rey,

Soe, S. Aust, 88. pp. LOI-1 10,

Gantrama, B., in Goarsenmn, M. F., and Pangixs, L. Wo. 1958. The Geoloyy of South Ans-

tralia. Jot, Geol, Bac, Anst, 5, pe 2, pp, 1-163.

Chir. J. M.. L960, MyTonitie rocks of the Moine Trust Zone in the Assynt region. North-

West Scotland. “Tras: Roy. Soe. Jidin, LS, pp, 74-03,

Dana, L., 1963, The fossiliterous Ciombrinn siccession an Meurien Peninsula, South Ans.

trala. Teeords S.A. Maus, 34, No, 5,

Lwouann, EL ON, 1935, Petrowraphic notes on intrusions of the Fonghton magma in the

Mt, Lofty Ranges. Trans. How, Soe S Aust, 59, pp, 1-15.

Barn, WS. Porsen, FJ. aml Vernooues, J, 1958. Metamorphic revetions wnd aneta-

morphic facies. Mem. Geol Soe, Amer, 73, 251 pp.

[96 J. L. TALBOT

Guucry, J., 1933. Replacement origin of the albite granite near Spurta, Oregon. U.S.

Geol. Surv. Prof. Paper, 175-C, pp. 63-81.

Grices, D., and Hanprn, J. (Eds.), 1960. Rock deformation. Mem. Geol. Soc. Amer., 79.

382 pp.

Hasucron, W.. 1960, Geology of northernmost Tennessee, U.S, Coal. Surv. Prof. Paper.

BLL, pp. 13-27,

Hinraxen, Anna, 1938. Petrology of the Finnish quartzites. Com. Geol. Finlande Bull.,

122, pp. I-LLb.

Hossretp. P. S., 1935. The geology of part of the north Mt. Lotty Ranges. Trans. Roy.

Soc. 5. Aust., 59, pp. 16-67.

Howcuin, W., 1906, The geology of the Mt. Lolty Ranges, Pt. II, ‘rans. Roy. Soo. S.

Aust., 30, pp. 227-262,

Howcuus, W,, 1926, The geology of the Barossa ranges and neighbourhood in relation ww

the geological axis of the country. Trans. Roy. Soe. S, Aust., 50, pp. I-16.

Kuveman, A. W., and Skixner, B, J., 1959. The Kanmantoo Group in the Strathalbyi-

Hinrogate region, South Australia. Trans, Roy, Soc. S. Aust., $2, pp. GI-71.

Kureman, A. W., and Warr, A, J. K., 1956. The structural petrology of portion of ihe

eastern Mt, Lofty Ranges. Jour. Geol. Soc, Aust., 3, pp. 17-31.

Ksopr, E., 1931. Retrogressive metamorphism and phyllonitization. Amer. Jour. Sei., 21,

pp. 1-27.

Larworra, C,, 1885. The Highland controversy in British geolowy, Nature, 32, pp. 558-4),

Mawson, D., and Sprice, RB, C., 1950, Subdivision of the Adelaide System. Aust. Jour. Sei.

13, pp. 69-72.

Sprice, R. C., Wrerrie, A. W, G,, and Campana, B., 1951, Geological Atlas of South Aus-

tralia, 1’ = 1 mile series. Adelaide Sheet.

Seay, A. FL, 1951, The Archaean Coniplex at Houghton, South Australia. ‘Trans, Roy. Sac,

S. Aust.. 74 (1), pp. 115-134.

Srankey, J., 1959, Chess-board albite from New Brunswick, Canada: Geol. Mag., 96,

pp. L41-L45,

Varn, G., 1960. New work on petrofabrics. Livy. Man, Jour. Geul., 2, pp. 503-567.

Weap, B. P., 1953. Structure of the Archacan Complex of Monnt Lofty Ranges. M.Se.

Thesis, University of Adclaide. 50 pp.

WooLnoucu, W. G.. 1908. Notes on the geology of the Mount Lotty Ranges, chieHy the

portion east of the Onkaparinga River. Trans. Roy, Soc. S. Aust., 32, pp. 121-137,

J. L. Taceot PLare 1

Orossed

Crossi

rans

[S244.

wy.

ita in the baund-

“Trans. Roy. Soe, S.A." Vol, S7,

AN EVALUATION OF THE CRUSTAL THICKNESS IN THE MARALINGA

AREA, SOUTH AUSTRALIA

BY I. A. MUMME

Summary

AN EVALUATION OF THE CRUSTAL THICKNESS IN THE,

MARALINGA AREA, SOUTH AUSTRALIA

by T. A. Musmiar®*

[Read 13 June 1963]

International geodetic gravity measnrements show that the earth's outer

crust Huats on an underlying substratam, which is referred to as the mantle,

according to the principle of isostusy. In recent years the discontinuity between

the outer crust and the mantle las been found to be a zone of seisrnological

discontinuities and is called the Mohorovicic discontinuity,

Seismological information suggests that the mantle has a constant density

of 3-32 grammes per ce, and the mean eruslal density increases from a minimum

valne helow the ocean of 2-86 grammes per ce, to 3-08 grammes per cc. beneath

the high plateaus and mountains.

Although geophysical and geologival work show that the earth’s outer ernst

is the region of greatest density variations, nevertheless, the earth’s crust is in

a state of isostatic balance and consequently a regulat relationship hetween

erustil density, elevations of continents and their associated vravity anomalies

Oceurs,

Tu determining the effective gravity unomally (which is expressed as a

Bouguer anomaly) for the Maralinga area, an average Bouguer gravity value

for a number of gravity stations established at approximately two-mile intervals

along the 13L° meridian from Fisher railway statiou to a latitude of 28°0’ was

ohlamed.

A World Wide gravimeter was used in measuring the yravity intervals

between the stations and because of the difficulty of access into the region a

helicopter was used in establishing the gravity stations occupied,

The average Bouguer anomaly obtained was — 40 milligals, and the average

elevation 570 feet.

These valnes were then applied in various equations and graphical methods

relating elevation and crustal thickness, and gravity anomaly and crustal thick-

ness, and are as follows:

(1) Applying Woollard’s method relating elevation and depth to the

Mohorovicie discontinuity, we obtuin a value of 34 kilometres for the crustal

thickness.

(2) Applying Woollard’s method relating gravity anomaly and depth to

the Mohorovicie discontinuity, we obtain a value of 36 kilometres.

(3) Applying the equation relating gravity anomaly and crustal thickness

nsed by the Russian and Chinese seismologists: H = 35(1 + tanh 0-00387 A ge),

where ET is the crustal thickness, and “\ ¢ is the crustal anoinuly, we obtain a

valne of 36 kilometres,

° Previously S.A, Mines Dept.; now Anstralian Ateraic Energy Corminission,

¥ p 7 ?

Trans. Roy, Soc. $, Aust. (1963), Vol, ST.

198 LA, MUMME

(4) Applying the equation relating gravity anomaly and elevation used by

the Russian and Chinese seismologists: H = 33 tanh(0-°38 A h — 0-18) + 38,

where IT is the crustal thickness, and A h is the elevation, we obtain a value of

34 kilometres.

(5) Applying Andreey’s formula H = 0-1 A g + 30, where H is the ernstal

thickness, and A g is the Bouguer anomaly, we obtain a value of 26 kilometres.

The average value of these independent determinations is 33 kilometres.

The scismic observations by Bolt, Doyle and Sutton give two values of

crustal thickness. From an analysis of the times of arrival of the P and S waves

from an atomic explosion, crustal thicknesses of 32:2 + 3 kilometres and

38-8 + 3 kilometres were obtained.

It can be seen that the application of Woollard’s elevation and gravity

methods, and the Russian and Chinese gravity and elevation cquations gives

values fairly close to the average value of those obtaincd by the scismic obser-

vations,

Andreev’s equation gives a somewhat smaller value for the crustal thickness.

The author wishes to thank Exoil Pty. Ltd. for permission to publish data

obtained while conducting a geophysical survey for them, and also thank the

Director of Mines for granting the permission.

REFFRENCES

Bour, B. A., Doyvie, H. A., and Surron, D. J., 1958. Geophysical Journal, Royal Astrona-

mical Society, vol. 1. No. 2.

Genson, S., and Van pe Linpen, J., 1957. Regional gravity traverses across the Eucla Basin.

B.M.R. unpublished report.

Mumm, I. A., 1963. Geophysical survey of the Officer Basin. Royal Society, Seuth Aus-

tralia.

Wootrrnarp, G. P,, 1959. Journal of Geophysical Research, vol. 64, No. 10,

MACCLESFIELD _

GEOLOGY OF THE

STRATHALBYN ANTICLINAL i]

AREA.

QUATERNARY

CREEK ALLUVIUM

TERTIARY

f 4 SANDS, LATERITE

CEMENTED QUARTZITE SCREE

fr CALC-SILICATE

NAIRNE PYRITE FORMATION

PYRITE SCHIST

ANDALUSITE SCHIST.

—_ SPOTTED SCHIST

PEBBLE BED

META-GREYWACKE, MICA SCHIST

[23] waccuesrieto QUARTZITE GRAQING

2] INTO META-ARKOSE,Coorse stippie)

ANOALUSITE-STAUROLITE SCHIST

QUARTZ-FELOSPAR-MICA SCHIST

[S] QUARTZ REEF.

PEGMATITE

‘| ZONE OF TOURMALINIZATION-

T BEDDING

“7 FoLATion

\) FACING

a 5’

\ LINE ATION.

;

Bra

Ny MINOR FOLD,

“Trans. Roy. Soc, $,A.”, Vol. 87. Fig. 1. Scale 2 inches to 1 mile,

STRUCTURAL GEOLOGY OF THE STRATHALBYN ANTICLINE

BY ROBIN OFFLER

Summary

Metasediments in the Macclesfield-Strathalbyn area have undergone at least two deformations. The

south plunging Strathalbyn anticline with minor eastwest crossfolds have been overprinted by two

sets of strain slip cleavage. Fabric relationships in the pelitic schists indicate phases of: pre-, syn-

and post-tectonic metamorphism.

STRUCTURAL GEOLOGY OF THE STRATHALBYN ANTICLINE

by Rosin Orrcer*

[Read 13 June 1963]

SUMMARY

Metascdiments in the Macclesfield-Strathalbyn area have undergone at least

two deformations, The south plunging Strathalbyn amticling with minor cast-

west crossfolds have been overprintecd by two sets of strain slip cleavage.

Fabric relationships in the pelitic schists indicate phases of pre-, syn- and

post-tectonic metamorphism.

INTRODUCTION

The area investigated is situated on the eastern side of the ML. Lofty

Ranges, approximately 23 miles south-east of Adelaide (Fig. 1), The rocks

consist of an extensive sequence of meta-arkoses and meta-greywackes with

minor cale-silicates, quartzites, pelitic and pyritic schists, They are strongly

deformed and are regionally metamorphosed under conditions of the middle

Almandine amphibolite facies (Fyfe, Turncr and Verhoogen, 1958).

A number of workers, including Sprigg and Wilson (1954), Kleeman and

Skinner (1959), and Horwitz, Thomson and Webb (1959), have examined the

area on a regional scale.

§ ADELAIDE

MACCLESFIELD

ST VINCENT

STRATHALBYN

‘CouNTER BAY

Fig. 2. Locality map showing the area mapped.

* Departinent of Geology, University of Adelaide.

Trans, Roy. Soc, S. Aust. (1963), Vol. 87.

200 R, OF FLER

South of Macclesfield, Kleeman observed lineations with a trend differing

from that of the regional fold axis. To investigate this relationship, the author

mapped this area in detail with cureful observation of structural style and the

various structural elements,

STRATIGRAPHIC SUCCESSION

The metasediments in this area are divided into five nnits and the successien

is shown in Table 1. The approximate thickness of the sequence varies from

1,500 feet on the west limb to 10,000 feet on the east limb of the Strathalbyn

uuticline (Fig. 1). These differences in thickness are thought to be due more to

sedimentary thinning than tectonic thinning.

Facies changes occur in the area. The Macclesfield Quartzite grades later-

ally to meta-arkose aud in the upper part of the sequence the meta-arkose

interfingers with meta-greywacke. The andalusite-staurolite schists commonly

tougue out,

Sedimentary features such as cross aud graded bedding, load casting and

current ripple marks are common.

Although the author disagrees slightly with the interpretation by Horwitz

et al, (185) on the placement of lithological boundaries and classification of

rock types, their stratigraphic nomenclature will be retained.

TABLE 1,

; Unit | Western Limb i Eastern Limh

ls | ee in Ee Ss Eh. .

5 Mota-provwwacke with minov pyritic | Mete-greywacke. cale-silicate.

= i | schists :

a | :

ae f dst be, ee hee _ ie NS eee

mis i t Nairne pyrite formation | Naitne pyrite formation

2 --——-

as . Cale-silicate Anilalnsite-staurolite stthist

1A 3) Andalysite-stunrohte sahist: prntic ane stuurolite-andalusito

Meta-greywacke with minor schists, pebble heds,

andalusite-staurolite schists

2 | Macclosfield Quartzite grading inte | Meta-arkose with minor quartzite

A mela-arkose | leuses: at buse.

ad. ps ech hem « | oi | pore

¥ ra | | duterbelded andalusite -struwolite | Interbedded andalusite-staurolite

me | achists and quarte-felspar-mica » achists and cniartz-foleparmraicn

aa ty | 1 . achisia with minor eale-silitea les schists with minor eale—

wD | i silicates,

STRUCTURAL GEOLOGY

Maeroscopic Strnetures

The structure of the area is dominated by a Jarge north-south trending

anticline called by Kleeman and Skinner (1959) the Strathalbyn anticline

(Fig. 3). The fold is assymetrie with a dominantly low dipping east limb and

a steep west limb. The axial surface of the anticline is sigmoidal in the central

part of the area where cross folding is present.

STRUCTURAL GEOLOGY. STRATHALBYN ANTICLINE, 5.A. 201

AXIAL PLANE TRACE

ANTICLINE ——

ARIICLINE OVERTURNED —ft-

SYRELINE 4

SUB-AREA BOUNDARIES == =

1S DiAGeAM

ae eo a a STATIST-CAL FOLO AKIS

7 A |

se # s man 8 siconparny £

, Pi / p

i / ! ;

‘. - J As’ . = 2") TRAST OF FORM SURFACE

% NN - STRATHALBYN \

"hg | tel ko So CONTOURS | 347% per \EASEA

Me . e 10 a0

SCALE TN CAINS

Fig, 3. Structural map showing major macroscopic structures and geometry of bedding, &.

202 R, OFFLER

Mesoscopic Structures

The term mesoscopic structure is adopted from Weiss (1957) and signifies

a structure seen in hand specimen or single outcrop.

Bedding (8) is banding vf sedimentary origin and is the most common

planar structure,

Foliation (8,) is comparatively rare. It is characterised by the preferred

orientation of muscovite and biotite in planes which have a variable easterly

dip (Fig. 5). In some localities, moyement parallel to this foliation has ruptured

quartzite bands to produce tevtonic inclusions (Tig. 4).

Fig. 4. Tectonic inclisions of quartzite parallel to foliation ‘1,

B,’ and B," are two sets of differently trending first generation folds com-

mon in the fold hinge of the anticline. Their somewhat variable axial plane

attitudes (Fig, 5, Pl. 1, Fig. 2) are indicative of a fold style commonly called poly-

clinal (Greenly, 1919). On the limbs of the B,’ folds, B,” crossfolds appear.

Lineations parallel to either of these fold axes are comparatively rare.

Crenulation cleavages Sz! and S./’ are two sets of surfaces of metamorphic

origin, which trend approximately north-south and east-west and parallel the

axial planes of micro-crenulations in § or Sj.

Axes of micro-crenulations Bo" and Bs” are due to the intersection of crenu-

lation cleavage with bedding or foliation and are thought to represent the last

phase of folding. The few small folds formed at this time have a similar style

ie 1, Fig, 1). The two lineations are commonly ussociated on the one foliation

plane.

STRUCTURAL GEOLOGY, STRATHALBYN ANTICLINE, S.A, 203

— .

oO a

Fig. 5 Fig. 6

Fiy, 5, Orientations of Sy (triangles), axial planes of By’ folds (dots), and axial plancs of By’

folds (squares)). Fig. 6, Total 2S for Strathalbyn anticlinal area. 440 total. Contours

1, 3, 5, 7 p.c. per | pie. area.

GEOMETRY OF S,

The 7S analyses of six sub-areas is given in Fig. 3. Each sub-area diagram

represents contoured equal area projections of poles to bedding («S$ diagrams).

B is the pole to the girdle drawn through the maxima and is a statistical fold

axis for that subarea. The main geomctrical features are:

(1) In all sub-areas, except numbcr two, the bedding has been folded about

a single fold axis B.

(2) Secondary girdles appear in all diagrams suggesting other fold axes

(p’) are present.

The collective diagram (Fig. 6) exhibits a strong girdle whose axes B

plunges 6° in a direction 172° and the statistical axial plane strikes 352° and

dips 84° east. S is spread along two other girdles indicating slight inhomo-

geneity.

Fig. Ta Fig. 7b

Fig. Ta, Collective diagram of By’ fold axes and lincations (dots) and By,” fold axes

(crosses). Fig. 7h. Collective diagram of statistical fold axes 6 (dots), 8’ (crosses), and

megascopic # (small circle).

2()4 R. OFFLER

GEOMETRY OF FIRST AND SECOND CENERATION FOLDS

The geometry of the different fold axes arc summarized in collective

diagrams, as no significant variations resulted when individual measurements

were plotted in the appropriate sub-area.

Geometry of the first generation. folds (B,’ and B,”), The orientation of

B,’ is almost coincident with the megascopic fold axis @ and the sub-area

(Fig, 7a, b) while the cross fold axes (B,”) vary in plunge and trend in a

similar fashion to ” statistical fold axes.

Geonelry of the micro crenulations (Bs’ and B.”), The following points

are noted in the collective and synoptic diagrams (Figs. Sa, b).

(1) The east-west trending crenulations (B.”) tend to spread along a partial

girdle (Fig, Sa),

(2) Bs! is close to the orientation of the megascopic @ and sub-urea g

(Fig. 8b).

Ey .

je ‘\, Aa

A ra) \, x

f J On

| )

| . . /

0} 5,

ra Z

eas — a

Fig. 5a Fie. 8h Fiy, 9

Fig, 84, Collective diagram. of Ba’ und By!’, 158 total. Contours 1. 3, 4, 7 p.c, per L p.c,

area. Vig. 8b. Synoptic diagram of statistical fold axes 6 (dots). A’ (erosses) and mewa-

scopic ® (small circle). Datted lines are 3 and 7 p.c. contours from Fig, 7a. Fie. 9, Cal-

lective diagram of crenulation cleavage, 60 total. Contours 1, 3,7, 11 p.c. per Lop.c, area.

GEOMETRY OF CRENULATION CLEAVAGE 5.’ AND 4,”

Sixty poles of crenulatiou cleavage are plotted and contoured (Fig. 9).

The north-south cleavage is more dominant than the east-west cleavage aud

shows a tendency to spread along a partial girdle.

DISCUSSION

Ju the previous summary of meso- and macroscopic geometry, it was noted

that fold axes determined from the +S analyses (@ and £') were essentially

edincident with the first generation, small folds By’ nad 8,”. This suggests that

the two sets of mesoscopic Folds are related to the two macroscopic fold systems.

Since 8, the statistical fold axis determined from the collective «S diagram

has a similar orientation to the By’ small folds, it can be assumed then that thev

are of the same age.

STRUCTURAL GEOLOGY, STRATHALBYN ANTICLINE, S.A. 205

Whether the B,‘ fulds developed contermporancously or not with the By’

folds can neither be determined geometrically from the available data nor from

field ubseryations, aus By’ und By” are not seen to overprint one another. The

variation of By’ axes may be due to variations in strain, superposition on an

early fold system or to slight reorientatinn by later folding. The lack of homo-

geneity of By,” axes suggests thut this minor expression owed its variability to

local stress inhomogeneities.

The micro crenulations are often seen to overprint By’ atid By” small folds.

Weiss (1959B) has shown that the axes of second generation folds are the

intersection of the new axial surface with previously folded bedding. Assuming

that in the Maeclesfield-Strathalbyn region, that 8S.’ and $2” (the axial planes

of the crenulations), have been superimposed on the first generation folds (By,

and By”) then the geometry of B.’ and Be” can be demonstrated diagrammatic-

ally (Fig, 10), The variation in the two sets of crenulation cleavage is repre-

sented as great circle sheaves which intersect bedding (stippled area), folded

about 6. Where intersection occurs, the second generation crenulations and

small folds are observed. 8 in the diagram is the megascopic fold axis of the

first generation. [t is assumed that in using this orientation, the movements

responsible for crenulation cleavage are only small-scale and did not affect the

overall orientation of the bedding (S$),

Fiy. 10, Superposition of crenulation cleavages $2’? and Sx’? on bedding already folded ubout

megascopic fold axis p.

206 R. OFFLER

FABRIC RELATIONSHIPS IN THE PELITIC SCHISTS

Several stages in the metamorphic history can be recognised in the pelitic

schists by comparing the internal fabric (Si)* of the porphyroblasts with the

external fabric (Se) (Table 2).

TABLE 2

Phase of Metamorphtism Irold) Moyement

Pre B,

Syn B,

Post 8,

“anualecons

Syn By

Post Ti,

Pre B, metamorphism as interpreted by Zwart (1960). is recognised com-

monly in skeletal andalusite porphyroblasts containing random inclusions of

hiotite, muscovite, quartz and magnetite. A later foliation (S or S;)) bends

around them, In most schists, augen made up of an aggregate of quartz, bivtite.

plagioclase and muscovite with no preferred orientation, are found between

foline (PL 1, Fig. 3),

Biotite, muscovite and mavuetite with strong preferred orientation parallel

to either § or S,, grew during the syn B,; metamorphic stive. Rotated porphyro-

blasts (Fig, 11) and quartz-biotite wugen (PL 1. Fig. 4) between S, foliac also

Vie. Uh. Twinned, svn. By staurolite porphyrablasts containing rotated magietite inehisions-

Foliation shows microtolding caused by Be movements. Section perpendicular iv By’.

2 After Sander (sce Fairbairn, 1949),

STRUCTURAL GEOLOGY, STRATHALBYN ANTICLINE, S.A, 207

suggest svntectonic crystallisation (ie. syn By). Lineation expressed by elun-

gated tracts of biotite formed in a few schists.

Evidence for post By metamorphism can be found in staurolite and anda-

lusite porphyroblasts: which have inherited 5,. The inherited foliation, often in

the form of biotite and magnetite, passes through the porphyroblasts without

deviation. During later fold movements (Be) some porphyroblasts containing

S,, underwent rigid body rotation (Pl. 2, Pig. 1).

The only positive indication of syn Bo metamorphism is shown by biotite

agercyates which have been rotated by differential movement along S$.’ (PI. 2,

Fig, 2),

Porphyroblasts that have formed alter Bs folding are qnite common. Idio-

blastic, pale pmk garnet always appears to grow from earlier formed staurolite

or biotite (Pl 2, Fig, 3) while muscovite replaces andalusite. Biotite and

chlorite porphyroblasts are found in mast samples entting across earlier formed

foliations (Plate 2, Fig.4). The last ta crystallize is fibrolite sillimanite whieh

replaces stanrolite, muscovite, andalusite and biotite.

RETROGRADE, METAMORPHISM

Retrograde metumorphism is present in all rock types. Chilorite (var,

pennine) replaces biotite and the titaniim oxide resulting from this breakdown

forms rutile in the {001} cleavage planes.

Sericitic coronas often sivroind the alurmino-silicates or cloud plagioclase

grains. Diopside changes to deep green hornblende, while scapolite breaks down

to xonublastic aggregates of clinovoisite or epidote,

DISCUSSION

The study of the internal fabric of various porphyroblasts and. their rela-

tionship to the foliations $. $) and Sy suggests that metamorphism las been a

vontiniious process hefore, during and alter the two deformation periods, The

presence of retrograde products indicates a re-adjustment of the mineral assem-

blages to lower pressure and temperature conditions.

CONCLUSIONS

Existing eviderce bas indicated that the Strathalbyn anticlinul area has

been subjected ta two periods of defurmation, During the first period the south-

plunying Strathalbyn anticline and associated cross folds formed, Limeation

and aw new foliation ($,), along with a continuance of metamarphism, accom-

panied this deformation.

Superposed. on the earlier folds are two sets of crenulationg whose plunges

are controlled by the intersection of cremation cleavage with the variable

attitude of bedding. Regional metamorphism continued during and alter the

second deformation,

208 R. OFFLER

ACKNOWLEDGMENTS

I am indebted to Dr, A. W. Kleeman and Professor A. R. Alderman for

suggesting this problem to me as an Honours project.

Dr. J. L. Talbot and Mr, K, J. Mills were helpful with advice on problems

encountered during the field wark,

The manuscript was read by Dr. B. Daily and Dr. J, L. Talbot and I am

grateful for their constructive criticisms.

Miss A. M. C. Swan was of great assistance with the drafting.

REFERENCES

Fyre, W. $., Tusnxen, FP. J., and Vernoocen, J., 1958. Metamorphic reactions and meta-

morphic facies. Geol, Soc. Amer. Mem., 73, 259 pp.

GrEENLY, K., 1919. The geology of Anglesey. Mem, Geol. Surv. Gt. Britain, pp. 1-980.

Horwirg, R. C., Tromtson, B. P., and Wrbs, B. P., 1959. The Cambrian-Precambrian

boundary in the eastern Mt. Lofty Ranges, Trans. Roy. Soc. S. Aust., 82, pp. 205-218.

Kieeman, A. W., and Sxinwer, B. J., 1959. The Kanmantoo Group in the Strathalbyn-

Harrogate region, South Australia. Trans. Roy, Soc. S$. Aust., 582, pp. 61-71.

Sprroc, R. C., and Watson, KR, B., 1954. Geological atles of South Australia, Sheet Echungu.

Wess, L. E., 1959a, Structural analysis of the basement system at Turoka, Kenya. Over-

seas Geology and Mineral Resources (Great Britain), 7, pp. 3-35, 123-153,

Wess, L, E., 1959h, Geometry of superposed folding. Geol. Soc. Amer. Bull., 70, pp. 91-106.

Zwanryr, H. J., 1960, Relations between folding and metamorphism in the Central Pyrenees,

and their chronological succession. Geologic en Mijnbouw, 22, pp. 163-180.

PuAave

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Dress

A TAXONOMIC REVISION OF THE GENUS MILLOTIA CASSINI

(COMPOSITAE)

BY RICHARD SCHODDE

Summary

The genus Millotia Cass. (Inuleae: Gnaphaliinae) is defined as comprising four species. One species

and two varieties are described as new. A key to, and descriptions, illustrations, and distribution

maps of the taxa are given. The systematic relationships between Millotia and allied groups of the

Compositae arc discussed, and a conspectus of the genera Millotia, Scyphocoronis and Toxanthes is

included. The annual growth cycle (germination to senescence) is outlined, and some of its features

are described in some detail.

A TAXONOMIC REVISION OF THE GENUS MILLOTIA CASSINI

(COMPOSITAE)

by Ricu#arp ScHonpE?

[Read § August 1963]

SUMMARY

The genus Milkitie Cass. (Timleac : Gnaphaliinae) is defined as comprising

four speeies. One species and two. varieties are described as new. A key to,

ind deseriptions, Mnstrations, ancl distribution maps of the taxa are given, The

systematic relationships between Millotia jd allied groups of the Compasitae

are disenssed, and a conspectns af the genera Millotia, Seyphecoronis and

Toxanthes is included. ‘he sinnual growth eycle (germination 16 seneseence )

is outlined, and some of its features are described in some cletail,

INTRODUCTION

In 1829, H. Cassini described the genus Millotia, with one species M. tenui-

folia, Irom specimens of a small annual composite collected by J. $. C. Dumont

d'Urville at King George Sound, Western Australia, The characters he quoted

to distinguish il were: all florets in the head tubular and bisexual; a cylindrical

involucre comprising “8 to 10” free uliseriate leafy bracts with a terminal

subulate point and membranaccous margins; a long, narrow, and scabrous “fruit”

with a pitted neck; and style branches terminating in conicul uppendages.

The genus has since been maintained by subsequent authors, and a further

seven species referred to it, namely, M, myvsotidifolia (Benth.) Steetz (1845).

M, glabra Steetz (1845), M1. robusta Steetz (1845), M. greevesti I. v. Muell.

(1862), M. kempet F. vy. Muell. (1882), M, depauperata Stapf (1910), and

M. hispidula Gandoger (1918). In Flora Anstraliensis (1867), Bentham treated

Steetz’s three species as synonyms of M, tenuifolia and Mueller’s eremean M.

greevesii as distinct. Later authors, such as A. J. Ewart (1931) and J. M.

Black (1929 amd 1957) of current State Floras, haye corroborated Bentham’s

taxonomy, and perhaps followed his lead insofar as the only species generally

recognised as occurring in Australia huve been M. tenuifolia, M. greevesii, and

M, kempei. M. depauperata Stapt and M. hispidula Gdgr, have not been

discussed in any publication since their origmal description,

METIIODS

Hersariv st

In addition to the fine series now preserved in the State Herharinm of

South Australia (AD), the collections of Millotia held by the follawing herbaria

were loaned for examination: Botany Dept. University of Adelaide (AD);

° University of Adelaide and State Herbartim of South Australia for the course of the

systematic work on Millotia; now Division of Lancl Research and Regional Survey, C.$.1.B.0.,

Canberra.

Trans, Roy, Soc. S, Aust, (1963), Vol. 87.

210) R. SCHOpDE

Waite Agricultural Research Institute, Adelaide (ADW); Botanie Museum und

Werburium, Brisbane (BRL); Commonwealth Scientific and Industrial Researel

Organization, Division of Plant Industry, Canberra (CANB); Staatsinstitut fiir

illgemeine Botanik und BKotanischer Garten, Hamborg (HBG): The University

of Tasmania, Hobert (HO); Botanisches (nstitut der Universitit, Kiel (KIWL):

Laboratoire de Botanique de la Faeulté des Sciences, Lyon (LY); National

Herbarium of Victoria, Melbourne (MLUL)—excliding types; National Lfer-

bartucn Of New South Wales, Sydney (NSW); Muséum National d'Histuire

Naturelle, Laboratvire de Phanérogamie, Paris (P): State Herbarium of

Western Australia, Perth (PERVIL), Dept. of Botany of the University, Sydney

(SYI>); Naturhistorisches Museum, Wie. (W). Di. R. Melville also kindly

submitted details of the collections of Millotia in the Kew herbarium (K), and a

sevies of seven sheets of Conyza Less. were loaned [or comparison hv the

lnstituto de Botanica Darwinion, San [sidro ($1),

The number of herbarium sheets that have been seen, excluding duplicates

and photopraphs, is 593: 215 slieets of Millotia tenuifolia, 300 of M. myosotidi-

folia, 72 of M. greevesti, and 8 of M. maerecurpa. The range of the series ol

specimens cannot be properly judged from the number of sheets because in

most collections more than one specimen is preserved on a sheet: recent entlec-

tions for the State Tlerburiim of South Australia, for example, comprise 10 te

60 oF more specimens per sheet und jue perhaps representative of local popu-

lations. Only types and selected collections which are representative or inter-

esting in their morphological variation or distribution ave enumerated as

specimens examined,

The types of all taxa have been studied, except those of M. greetesil and

M. depauperata which are held by the Kew herbarium. Detailed deseriptians,

drawiags and photographs of these latter types were furnished by C.S.LR.O.,

Canberra, and Kew,

Fim ANp. LAvoRAVONY

The following species were observed and collected in the field: Milletia

feniifolia (both varieties). M. sayosotirlifolia, and M. ereevesii var. helmsii,

M. tentfolia var, tenvifotia and MM. fennifolia var. nudescens were fairly inten-

sively sampled in the Chanucey’s Line area near Murray Bridge at quarter- to

two-mile intervals alung two road transects six aud ten miles Jong luring

Augtst-October, 1958, a project resulting in the collection af over 2,200 individual

plants. The aim of such sampling was to determine the morphological) variation

in cavh Tocal population.

The seasonal growth cycle of M. tenuifolia and M. myosotidifolia was closely

inspected in the field. lor this, consistent visits were mude between Mav and

late October, 1958, to various sites on the Adelaide Plains, central Mt. Lofty

Range. and western Murray Mallee, and successive growth stages were collected.

AL tenuifolia. M. myosottdfolla and M, macrocarpa were gown from ger-

minated seedlings in glasshouses at the Adelaide Botanic Garden, No viable

seed of M. greevesii was uvailable, Toxanthes muelleri and Quinetia arvilled

were similarly grown for purposes vf comparison. The germination itself was

eflected on dises of moist filter paper in a series of constant temperature incu

hators at the Zoology Dept., University of Adelaide. Seedlings of Millotia tenui-

folid which had been transplanted from the wild state were also grown, as in

the cause of var. dennifolia and yar, niudescens feorn Channcey’s Line, All plants

grown in the glasshouse have beon preserved as herbarium specimens.

TAXONOMIC REVISION, GENUS MILLOTIA CASSINI 301

While the taxonomic results of this study are based on the examination of

herbarium specimens, investigations of living plants in the field und glasshouse

lave provided useful confirmatory evidenco, and though the taxonomie deserip-

tions are deawn from herharinm material, the characters vf corolla colour. scent

wid cotyledon shape are taken from living plants,

TAXONOMY

Millotia Cassini, Aon. Sui. Nal 17(1829) 31,416: Cass. Dict. Sci. Nat. 60(1830)

579,a92; Less. Syn. Gen. Comp. (1832) 273, DC., Prody. 6(1838) 161;

Fadl. Gen. Pl (1838) £45; Meisn., PL Vase. Gen. 1,1 (1839) 219: Walp.

Kop, 2(1h43) 645: ibid. 6( 1816-47) 234) Took.f, Vl. Tasm. 1( 1856) 200,

Benth. Fl Austral, 3(1867) 595; Benth. & Hook.f, Gen. Pl. 2(1873) 315;

Johnston, Memoravd. Tasm, Bot, (1874) 24; Spicer, Tandh. Pl. Tasm.

(1878) 27; Iv, Muell., Trans. Roy. Soe. N.S, Wales 15 (1881) 216; Baill,

Hist, Pl. 8 (1882) 177; Fav, Muell., Syst. ens. Austral. Pl. (1852) 82:

Moore, Cons, Pl N.S Wales (1884) 37; Fa. Muell, Key Sysi, Vie. PL

1 (1887-1888) 337; Fiv. Muell, Sec, Syst. Gens. Austral. Pl. (1889) 135:

Hoffm. in Bngl, and Prantl, Nat. Pilanzenf. 4,5(1890) 191; Bailey, Cut, Pl.

Queens). (1890) 25; Tate, Hundb, Wl, Extratrop, S. Austral, (1890) LIV:

Baill, Diet. Bot. 3 (1891) 361; Moore & Betche, Handb. FI, N.S. Wales

(1893) 296; Bailoy, Queensl, FI, 3 (1900) $43; Rodway, Tasm, FI. (1903)

84; Sulman, Guide Wildf. N.S. Wales 2 (1914) 83; Maid, & Betche, Coens,

N.S. Wales Pl. (1916) 201, Black, 11. S. Austral. (1929) 638; Fwart, FL

Viet, (1931) 1130; Gardner, Enum. TP Austral, Oec, (1931) 134; Lemée,

Dict. Gen. Phan. 8b (1943) 885, Black, FL S. Austral. ed. 2, (1957) 916,

‘Type species: Millotia tennifatia Cass,

Annual, grey to virescent, slender herbs, 1-20(30) cm tall. Stems, leaves.

yedimeles, and midvibs of involueral bracts covercd with a -+ dense whiksh

Jannginose indumentum, sometimes with pilose or short glandular fairs. Boer

simple. Stems slender, + branched diffusely at or near the hase rarely simple,

erect or ascending or decumbent. Cotyledons linear to almost filiform, + evenly

recurved, 2-7 rin long. glabrous though sometimes hispidilous, usually with a

+ conspicuous terminal whitish eap. Levres cauline, erect. alternate or becar-

or yellowish glabrous mucra, Pednneles + conspicuous, (42)2-8(11) cm long,

und exceptionally + absent, occasionally bearing 1—- several + subulate herba-

vents Ieaves 2-8(15) min long which may grade into the canine leaves, In

oalueres cylindrical, (3)4%-8(10) mm long, with a uniseriate or less conspicuens

hiseriate whorl or (3)6-14(20) linear to broad oblong free tion-radiate bracts

with herbaceous midribs and scarious margins and apices. Receplacle naked,

pitted. Florets all tubular and hermaphrodita. Corallas tubular to funnelfornn,

2-5(7) mm long, ereamy white to yellow, the corolla Lubes ereet or bent below

the throat which is deflexed over the top of the mvolucre, usually bearing sparse

minute glandular hairs, Stamens 3-5, the anther auricles with fine ciliate tails,

Pollen grains spheroidal to spheroidal-oblite, + 15-25 », diam,, tricolporate, with

a spinous exine. Sfyle apices acute to narrow obtuse and dilated dorsally with

dense papillae to form expanded cone-like appendages. Cypyelie variously

papillute with the testa wall closely striate, + Irear, 3-12 mm lone, brownish

ta dark reddish-black, with a conspicuous bewk, and very shortly stipitate.

Pappas dull white and various, of a ring of barbate setae, or of = plumose setae,

or Of smull scales, or absent.

212 R. SCHODDE

— The name “Millotia” commemorates Claude Franeois Xavier Millot (1726-

1785), a French historian.

DisTawvrio~n agp Lcococy

Confined to Australia south of the tropic of Capricorn (exchiding the east

coast and Great Diyiding Range north of Victoria), and Tasmania,

All species grow in sund or essentially sandy soils, That pollination is

apparently camied out by insects may be deduced from the type of pollen

grains and aromatic Hower heads or herbaccous parts, Dispersal of pappuse

cypselae may be effected by animals and ta a lesser extent by wind. However,

in the three species observed in the field, almost all eypselac of both pappuse

and apappose types were shed directly on to the ground around the parent plant.

All species are annuals, in southern Australia, seeds germinate with the

ariset of winter rams, usually in April or May, and the plants grow slowly diriny

winter. Flowering takes place from (Junc) August to October (December).

In M. tenuifofia and M, myosotielifolia, the times of flowering for local popula-

tions appexr to be approximately the same each year, irrespective of variations

in the seasoms, such as in raimfill which affects vegetative growth appreciably.

Ini arid Australia, the cycle of germination and development is: similar but

more erratic and the Howering generally earlier, M. greevesii and M. meagro-

carpa, which grow in the regions with irregular or mainly summer rainfall

(Burbidge, 1960, Pig. 1), lawer consistently between July atnd October. It

appeurs likely, therefore, that these species have arisen from temperate ancesturs

and have retained a life cycle with winter growth.

GERMINATION

The results from germination experiments in incubators are: No seeds

germinated at temperatures above 21° C.; + all viable sceds germinated at

temperatures below 15-6" C, The 12-3-18+6° C. range produced the highest

germination percentages and fastest germination which was from 6-14 days in

all species; no significant differences were noted between the species in their

responses, This temperature range corresponds in general to the day tempera-

tures in the southern districts of South Australia between April and fine. Cer-

mination percentages averaged from 70-100 p.c. tor M. fenuifolia and M. myosa-

fidifolia, and from 40-50 p.c. for Af, macrocarpa, and varied considerably between

local populations af each species.

vermination will occur only in a moist situation. On wetting, the cypsela

papillae in all species dissolve and form a colourless glutinous jacket over the

cypselae. The probable function of this jacket is to fasten the cypselae te

sumramding soil particles during germination,

In all species grown, the radicle emerges from a slit on the side of the

cypsela, usnally near the base, Jn associated genera, the radicle usually pene-

trates through the base in Voxanthes (T. muelleri (Sond.) Benth.) or from a

slit on the side near the apex of the eypsela in Quinetia (Q. urvillei Cass.). The

cotyledons of Toxanthes are more sharply recurved at the apices than those of

Millotia, and those of Quinetia urvillei are Heshy and almost straight.

Tricotyly was observed in one specimen of Millotia tenuifulia germinated

from seed collected by P, C. Wilson (894) from Kangaroo Island.

TAXONOMIC REVISION, CENUS MILLOTIA CASSINI B13

‘Vaxonomic: ReLatoxssirs

Cassini a referred Millotia to the subtribe Cnaplatliinae, tribe Tales,

# pusttion which has been corroborated by later authors such as De Gandolle

(1838) und Hoffman (1890), and also Lessing (1832), Bentham (1873), and

Lemée (1943) who subdivided the Gnaphaliiaze further and placed the genus in

their group Ilelichryseae, The characters of the genus confirming this latter posi-

tion are its woolly indumentum, scarious-nrirgined bracts, homogamons-discvid

Hower heads, and tailed anthers; its closest allies are also members of the Heli-

chrysene,

Characters of Millotia anomalous in the Gnaphaliinae-Inuleac are the 4

nniseciate iInvolucre, homogamons-discnid flower heads, conical stigmatic append-

ages, aud heak cypselae, even though other members of the Helichryseae possess

one or more of these features, Similarities have been noted between Millotia:

and other genera outside the Luuleac, for example with Erechtites Rafin,

(De Candollo, 1838) in the inyolucre, and with Eurybiopsis DC, (Hooker, 1856)

aud Conyza Less, in the habit. Bentham (1873a) even noted that AMéllotia

connected “in some measure” the Helichrysexe with the Senecioncae, because of

its “almost uniseriute involucre”, ‘This’ possibly explains why he described

M, nyosotidifolia first as a Senecio. Cassini (1829) and De Candylle (1838 )

saw in the beaked eypselae affinities also with Chenreulia Cass. (of Bentham’s

Eugmiphalieae group), a South American genus which is quite distinct on

account of its perennial habit, several seriate involucre, and heterogumous

flower heads, The similarities are, however, in isolated charucters only jindl

of little consequence.

Within the Helichryseae, the affinities of Millotia have heen diseussed by

several authors. Reutham (1867), then Bailey ( 19(X)) stated that Millotia dif-

fered fram Leptorhynchos Less,, and Wattsiz Wendl, in its non-radiate involucre,

and from other Gnuphaliinae in its eypscla beak. Mueller and Tate (1896),

and Black (1919, 1927, 1957) noted that Millotia preevesii subsp. kempet re-

sembled Tuxanthes Turez,, though their observations were based on the general

absence of pappus, a character which is strikingly variable in Millotia.

lt is well kriown that the limits of many genera pf the Compositac ave

diticult to define; Millotia is na exception. Tt seems that Millotia is allied to

Txivlaena Benth. and possibly Wailsia (and thence other genera with radiate

involucres) through M. myosotidifolia on the owe hand, and to Seyphoceronts

A: Cay through M, tvvevesii and to Toxanthes through M, lenuifolia on the

other.

The affinities between Millotia and Ixivlaena, whieh lie in the woolly uften

glandular indumentum, the pedunculate and homogamous-diseoid flower heads

the morphology of the iuvalucral bracts and deflexed corollas, are not uevat,

Significant differences in. Iviolaena ave ity larger size, perennial hwbit, multi-

seriite involucre, truncate style branches, and smooth unheaked cypselae.

The relationship between Millotia, Scyphocoranis, and Toxanthes, ull of

which are confined to Australia, is far more complex, Outstanding is the striking

vartation in pxppus in the three genera. Features common to each are the smull

annual habit, = uniseriate involucre, homogamous-discoid flower head and +

deflexed coralla; the distinguishing characters are given in the following con-

spectus:

214 R. SCHODDE

1. Millotia Gass. S/ahif + open. Stems conspicuously and densely woolly, rarely

sparsely woolly, Primary stems unbrimched, or with several Iateral branches usually near

the base. Leaves alternate. Flower heads conspicuously peduaculate. Ineolucral lracts

ca. 6-14, free at the base, with conspicenous searious margins, Corollas tubular to fuinel-

form, the Joni remaining cream to yellow after anthesis, the tube erect, or straight and

sharply bent below the throat fa detlew the coralia. Style branches with broadly acute te

expanded conical tips. Cypselac muricate or with + striguluse papillae, eypsela beak present

and straight, cwely slightly: curved at the apex. Pappus of bristles, scales, or absent,

2. Seyphocoronis A, Gray (1852). Habit + dense. Stems amd leaves without wool,

or sparsely and not vonspicuously woolly, Priavary stems with numeroans_ juteral heuiches

(en, 3-LO} ti hush specimens, the laterals most frecpient nerr and above middJe af primaries.

Leaves opposite, sirb-opposite, or alternule, Flower hedds subsessile and surrounded by

cathe leaves. or conspioiously pednnentite. Involueral Jracts 3-8 (10), connate or free

at the hase, with or without inconspicuous seariaus margins, Corollay tubular aud fume!

form; the limb hbecouing pink-rod on remiainise yellow after anthesis; the tube curve!

through its whole length or Dent below the throat, Sile branches subulate or witly ae

panded conical tips. Cypselae with glandular papitlie; cypsela beak wosaut, Pappa absent:

conspiotons cup crowning evpseli,

3. Toxanthes Sures. (1851). Herbit + dense, Sterns sind deaves without wool or

spatsely wonlly. Primery stems with oimerous lateral branches in Insh specimens, ay in

Seyphocoronis, Leaves usnally opposite, rarely sub-upposily or alternate, Flower heeds

aatmartiie wud surrounded by cauline leaves. Tneolneral brtete oa. 3-5, connate at base, with

ar without narrow -scicious anargins, Corollas tubular; the dah becoming pink-red after

anthesiss the debe curved through its entire length. Style branches subulate, Crpscloe

with ghindular papillae; cypsela beak present, a curved Unrongh ils length. Pape Cap-

purenth:) of - dense wool, or the corolla base ghibrous or abrist so.

Despite the separation of these genera in the cuuspectus, Seyphocoronis

majus (Turez.) Drace seems ta be morphologically identical with Toxanthes

mnelleri except for the eup crowning the cypsela. There is also an undescribed

ypecies from the arid regions north of the Nullarbor Plain (N. Forde 409; AD,

CANR: and Elder Exploring Expedition: AD95732062), the characters of which

have been incorporated under Seyphacoronis in the canspectus, and which has

the bahit, indumentum, and mvolucre form of Toxanthes, the apical eypsela cup

of Seypltoveronis, and the alteynate leaves, peduncles, free bracts, and floret form

found in two species of Millotia, particularly Mf. greevesil.

Notwithstanding the intricacy of these relationships, Millotia, Toxanthes

and Seyphocoranis are not united under one genus here because (1) together

they would form a taxonomically winvieldy grouping, with an wnusnally wide

range in infra-generie variation, (2) the species of Millotia still form a inest

diserete alliance am their own, und (3) the delimitation of AWilotia in its cus-

tomary sense is in aceord with the generic limits recognised by Bentham (1873

his) amd Elofinan (1890) in this group of the Compasitie,

Kev ro tie Spucivs§ axh [xerna-specivic Taxa

ta Goeolke Tinh af 5 Diregstioaiaths 4d) aeule, abnost attenuate lobes whieh are 14-45 am

lenis. Anther theeae oblong, 21's nim long. Connective apices exserteedl prowinent)

lwwound the lithh at onthesiy.

bo -Cypselae + strimmlose, Le. with oblong-chiyate: appressed papillae which are minutely

bifid at the apes. Leaves ® ublanecelate to narroy oblanceolate. Pappus of Anely

toothed sete ot. ws Jong as ceralla. Midrib of involucral bracts carinate, as Trovl

as or murower than suirious wargis, Corollas creamy white, rarely creamy yellow.

tT, AL, muyeurtieltfotia

Mh Cypselac papillate, te, with short romaded or conical papillae. Leayes maitrow-lineut

to ae Aldorm. Pappus of plunose setae = ht as Tong as corolla, of ratte scales. or

absent. Midril of involoeral braets aaviewlar, -& twiee as broad ns seurlous anuryin,

Gorollas bright yellow. 2 OM, greevesti

TAXONOMIC REVISION, GENUS MILLOTIA CASSINL 245

Sn Pappus of 10-20 plumose setae + 14 as long as corolla. Beaks of inner eypselae

usually protrading more than 1 mm above top of inyolvere- {

(Mf. greevesit subsp. greevesii’)

4a Involucral braets appearing connate with a dense laguginose indinnentum,

without shuncdula hairs.

M. greevesii subsp. greenesii var. greece yit

4b Tavolucral bracts distinctly free, with a @landular and -— woolly inehimentuny,

M. greevesii subsp. greevesit var, alanilulosee

3b Pappus of iinate scales or absent. Beaks of inner eypselac rarcly protruding to

lanm above the top of fuvolucre.

(M. grecuesti subsp, kempet)

fa Involueral bracts with dense lauuginose indumentum only,

M. vreevesii subsp. kenipet var. kempei

5h Involucriad braets with a glandular and + woolly indumentum.

M. greeresit subsp, kempei var. helmyii

1h Corolla limb of 3-- (exceptionally 5) + obtuse or hardly aente lohes which are (44)

Ty-ly (45) am long. Anther thecac elliptie, (44) 424 (46) nnn Jong. Connective apices

vnclosed, or only slightly protruding from the limb at anthesis,

fi Tndumentim af dense woolly hairs only, Cypselae partew-linear, (7) + 10 (12) mm

long, the Leaks protruding (1) 2-3 (4) mm. above top of involuere at maturity.

Corolla narrow cyathiform, the link 3- to 4lobed, spreading ut anthesis. Pappos

of semi-pliinose setae. 3. MW. maerocarpa

6b Tadumentuin of woolly and straight hairs. Cypselae linear-clayate, (3) 4-6 (74) wm

long, the bextk apiees + level with top of involucre at maturity. Corolla + tubular,

the fib 4-Inbed (exceptionally 8- or 5-lobed), aud + erect. Pappns tever semi-

plamase. 4. M. tenuifalin

Ta Pappus of ca. 20-30 fine setae, +b as lone as corolla, Corollas + erect,

M. tenuifolia var. tenwuifalia

Tb Pappus reduced, varying from a ring of 20-30 (40) setae of unequal Jenuth and

up to = 24 a8 luny ax corolla, to =F S unequal setae in nuniber, ar a river of nrinute

sexles im size. Corollas + dellexec.

M. tentifolia var. nudescens

Millotia myosotidifolia (Benth,) Steetz in Lehm., Pl, Preiss. 1(1845)457;

Walp. Rep, 6( 1846-7 )23-4; Sonder, Linnaea 25(1853 )502-3; Tlannaford, Notes

Fl. & Faun. Vict. (1856)61.

Senecio myosotidifolius Benth. iu Eudl,, Enun. Pl, Higel. 1(1837)66; D.C.

Prod. 6( 1838 )371.

Millotia glabra Steetz, in Lehin., Pl. Preiss. 1(1815)458; Walp, Rep. 6( 1846-7)

24.

Millotia robusta Steetz iu Lelim., PL. Preiss, 1(1845)458; Walp. Rep. 6( 1846-7)

O34.

Millotia myosatidifolia var, robusta (Steetz) Sonder, Linnaea 23(1$53)503.

Millotia myosotidifolia var, glalirescens Sonder, Linnaea 25( 1853 )503.

Millotia tenuifolia (non Cass.) Hook.t., I. Tasm. 1(1856) 209 p.p.; Benth,

FL. Austral. 3 (1567) 596 p.p.; Johnston, Memorand. Tasm. Botanists (1874)

HH ? pps Spicer, Handh. Pl. Tasm. (1878) 27, 117 p.p.; F, v. Muell,, Trans.

Roy. Soe. Tasm., Rep, for 1878 (1879) 17 p.p. Tate. ‘Trans, Roy. Soc. S$.

Austral, 3 (1880) 72 p.p.; Fav. Muell., Syst. Cens. Austral, Pl (1882) 82 p.p.:

Moore, Cens, Pl. N.S. Wales (188+) 87 pp; Fiy. Muell.. Key Syst. Vict. Pl.

2 (1885) 34 p.p.; Fv. Muell., ibid, 1 (1887-8) 337 p.p. Fv. Muell., 2nd

Syst, Cens. Austral, Pl. (1889) 138 p.p. Tate, Handb Fl. Extratrop. 5.

Austral, (1890) 119, 239 p.p.; Moore & Betche, Handb. Fl. N.S. Wales

(1893) 286 p.p.; Rodway, Tasm. Fl, (1903) 84 ?p.p.; Diels & Pritzel, Fragin.

216 i. SCLHIODDE

Phytograph, Austral. aec. (1905) 616 ? pyp,; Dixon, Pl N.S. Wules L (1906)

187 p.p.; Sulman, Guice Wildfl, N.S, Wales 2 (tel) 53 ?p.ps Maid. &

Betchu, Oens: NS. Wales Ph (1916) 201 pip. BN. Club Vict. Cens, Pl.

Viet. (1923) 67 pps Cleland & Black, Trans, Ray. Soe. 8. Austral. 51 (1927)

39 prs Black, FL S, Aanteal. (1929) 638, F291 p.p. Bawart, PL Viet. (1931)

1139 p.p.; Gardner, Enum. PI. Austral, Occ. (1931) 134 ?p.p.; Black, FI. $.

Austral, ed, 2, (1937) 917, £1215 pp.

Miflotia depauperata Stapf, Kew Bull. 1910(1990)22. “Millollia depinperate”

‘The Kew specimens, which were seen from a photograph in CANB (Neg.

Nis Kew 1636, 10.12.1953) are to be treated as the holotype because their label

beurs the name “Swan River", Hie only locality cited by Bentham in his original

description. The specimens in both herbaria are identical in appearance and

stave of development, and probably constitute a single collection, Tle vollec-

tion in W is therefore considered an isotype.

Crey, ravely vireseent herh, (1)4-16( 30) em tall, (1)2-12( 30) em

broad. Indumentum white linuginose only, of variable density, very woolly

or floecose in sorne specimens to + absent in others, always densest ut the

apices of the peduncles enhancing their expanded appearance, Sfeyns 1-10( 25).

ascending or sometimes erect with a central leader, more robust than in any

Uther species and usually thickened at the base. Coftyledons (3)4-6(7) mn

long, the tips slightly recurved. Leaves narrow to broad oblanceilate or ouca-

sionally spathulate, exceptionally oblong or linear (except the first leaves ubove

wotyledons and the uppermost: leaves at base of peduncles), (%)2-4(8) em

long, (1) 2-5 ( 8) ram broad (at the widest part), = mucronulate, conspicn-

dusly amplexieaul, relatively sparse and often appearing basal due te the long

prominent peduncles, Flower heads (1)5-30(200). Peduneles (44 )2-8( 12)

em long raising the involucre (0))144-6(9) cm above the tops of cauline leaves,

becoming relatively stout at maturity, appearing slightly expanded below the

involucre, Tnvolucres (3)5-7(10) mm long, of (3)8-13(20) + biseriate and

basally imbricate narrow to broad oblong bracts with carinate midribs usually

narrower than the broad, straw-coloured or sometimes red-purple margins: bract

upices caudate rarely acuminate or acute, + entire, sometimes recurved, olten

red-purple, Flower heads with ea. (3)15-45(100) dorets, honey-scented,

lorallas fieltorn, (2%)3%-5(7) mm Jong, deflexed over involucre (peri-

pheral corollas most deflexed, innermost corollas usually = erect), creamy white

rarely creamy yellow with the duibe becoming brownish to reddish brown after

anthesis; corolla limbs of 5, exceptionally 4, + spreading acute to almost attenuate

labes 2-44 mm long, Stamens 5, with tips exserted beyond corolla limb, anthers

with oblong theeae (%0)%-L6(1%) mm long, the connective Hp extending

(47804904) mm beyond theca; pollen grain diameter ca. 20-25 p, Style

branches (1)1%-115(2!%) mm long, with acute broadly dilated conical append-

ages at the apices, Cypselue + striguloxe, linear rarely oblong, (3)4-8(10) mm

Jong and protruding up to = 2 mm above top of involuere at maturity, entirely

pale brown fo brownish black; eypsela papillae > relatively sparse, oblong-

elayate, 3-0 mim long, appressed, shortly and acutely bifid at apex, transparent

or white translucent but sometimes reddish-brown at base; cypsela beaks (4)

1.5(5!) mm long, compressed to rarely broadly compressed, distinctly de

magreated, with pupillae + restricted to margins, Pappus of (15)18-25(30) —

exceptionally fewer and rudimentary — erect barbate setae which are = as

long as corolla though often slightly sharter, and with the teeth nsually longer

and denser at setae tips (Fig. 1).

TAXONOMIC REVISION, GENUS MILLOT IA CASSINI 217

Fig. 1. Millotin myosotidifolia {Benth.) Stectz, A, whole plant (Schodde 956)5 B,

iovahira bract (type Hagel: W); C, flawer head (Schodde 956); D, florets with maturing

cypselae (1,2 = Schodde 1010, bbs 3 = Whibley 401); E, whole style and audroecium just

after anthesis (Schodde 956).

twu

_—

RK. SCHODDE

Srruimias FXAMINER

Wesiekn Avuareviia: — Anonym LL: ADOST240LL: Rottiest. — W. Mi, Blackall 2631:

PEWTH 1582/41. Dongarra, L6.1X.1932, — Carey: MEL: Goograph(e) Bay. — fh 8. Clotaned:

NSWALT78: Cunderdin IXd908. ~ Dempster: MEL, (2 sheets). Between Esperanve Bay

and Proser's Range, 18768. — J. Prummond 365 (probably 5th collection): MEL, Ws:

WoOAL (MEL), Nov. Holl, Aust. vew. (W). Pon Th44. — WL OV. Fiteneralel: NSWa1 TH:

Bowler. 1X.1895, pop. — C. A. Gardner 560, R569: PEWTO gone Neat Wiluna, VILL193.

pp. — B. PT. Coadly 206; NSWalT90; Mt. Barker, X.1900, — Aleals MiSs 1. sourees of

swan Hiv(er)., 1689. pip. — A, flefis; ME, N.S.W,41873; Pinkaa, Murray 2. 23.04.1927.

— pee A. Helias; PERTH sour Riuridule, X898. — fitivel: Wosme Fremimtle. (type ol

Senecle muyosatidtfelins Benth). — J. Fl, Alaicden sic ADYS727060: Bussellon, N.L90H, —

AL Morrison; LY: Kebnscott, Canning (iver. 1OEXT898 pp. — I. Mueller; MEL:

Mainelin-Jtarboor, Shark Bay. N.T877, — FL Mueller: NSW4L795S: Stirling Range, —

Moir MEL: Lake Moin. Oltfelil> MEL (2 sheets), W Acqua. T889 Ne. 36953: Murchison

R. Oldfickds MEL: “Tone River, — Preiss 100: MEL, (2 sheets}: In valley neue Jake. Rote

nest dskind (Swan River Oolony). 22-VIILESS9, Clype ol Milletia glabra Steele amd a

muyosotidifilla vars glebreseens Sonder), — Preiss GBS HBG, KIEL252/7, MML (2 sheets 1.

Po W (2 sheets: Acqu. T8890 No. 130056, and sand: Tie Relde about Merth (hwan River

Colony. 27IX18AG, Ceited by Steets, (415), Preiss G7: MEL, (2 sheets): Interior

District Plantagenet (Swan River Colony). NTO, (tgpe of Milatia vabusta Steete |. —

Q Pritsel 345; NSWALTO. Wo Acqu. THO No. 7082: Shiurks Bay. VULLGNL - RD,

Reyer 1207: PERTH LIGOO/44: G nailes cust of Ballicds HIN DO4EG. py — TP BL Stier

any PEKVH sar Bussellon, LYLe.

Sournm Ausrnanmar — ALWLAL (= TF. W. Andrem): ADYSTSIOL8> Hluckbeath, nr:

Mirtvgate, 24 N 1918 — Avuonyorn (Herb. HK. Tate): ADYaT2Z401G. Mt Parry Roeks. —

anongin, (P Behr): MEL: Kl. C= Kangaroo Ishind) (Ticdler’s section). NT, — Anonyne:

MEL: Collius Bay — EB, Ashby 1OkO: NSW41792: Middle River, N.W. Kunnirva Js. 4.1905,

=f, F. Boelim aaa ADWATI1: Sotherlands, U%.1931, — JB. Cleland say; ATI95TIN0ST

ALK Weele, 20 ioiles qorth of Eiistun, 22, ViILd825. — My. Bickley 12478) ADYSTINGIS,

Couinion Ranges. Near mouth of @arge of Arcoona creck south of Avcoona Blu Bunge.

L7IX.1956. — Uj, Bieliler (4000. ADOBTIIOGS: Between Corny Point and Cappy Spencer.

Cw 17k ko. south of Corny Point. 360N.1957, — 1. Blehter 14227; ADYSSO8059; Seroh

hetween Stansbucy aid Minkiten, ca. G kaw north-west of Stonsbarv, 2.XLP57. - FLA

MHitin 665: ADWIOLSS: SAW. Bookoloo, Yoduapinin Sti, IVIL T9S- — f. Ly Massey:

MEL: Port Filiot. J893. — BE, H. bying 632: ADYSS17035; Moologloo Stn. X.LILS, —

die AF. desta yon: AD95$33159: ‘Tareogla, 21.04.1920, — RB. WM, Ista sony ADYSSSSLSS:

Huekharm, TON,1988, - 1 A deine sang ADDSSITOIT, ADYGOOSDOL: Waterfall) Gully.

12N01082. — BF. Hy fsiuy sine; ADYSS17034; Wadedikes Bock, 2.X.1L995. — BL 7D. Esti se

ADY58339156. Wiadinnas, EP. 20,1X.1939. — BO NOS, fuckson an: ADYSUISLO0: Telowie

OO Krachenbuebt 18; SDYBWO90EY; On cocky Dillslopes of the old Blianan Gopper tine

wth en of Blimima, 4.4.1958, — Wo, Latehfiekl: ADWS892; Al, Stiding, Upper sth-eist,

NA5Q — FL vtuellers MEL: Gaielen Buy, I8t8 TUB. | TO & Paltriptee);

\DOSTAqNO8; Bomtbumbie Springs. Neonunore, 23.VE,1930, — Bo Solute 504;

ADYSKITIOL: Golden Grove, ca. 16 kr north-cast of Adelaide, S.MIUS7. — RB. Sehaddde

956) ADO5S90808L> The Pinery, Adelaide Plains. 3.X.1954. — B. Sehodle TOUB- ALERDONORY:

South side of Channeey’s Line, ea. + kin south-east of Hartley, S2.N.L958. — J. GLO),

Tepper 275; ADS5NNSL22, MEL: Clarendon, Coromandel Valley. UNLISS1. -— D. OE.

wh wey 401: ADYSVO9NGB: Gawler Range, Hill behind Yurdea Station. L7.X.1958, ~

L, 0, Williams 2: \DYS919001; Meninuie, ‘7X.EN55, Po. Wiley 290; ADSFINGO6-4,

Hosten Tyla, mr. Port Lineokn 8.X. 1958. BG, Wilson 102th ADOSHINOSL: Jidlia

Thine, en, 168 kay nerth of Adelaide. LL NUL95%.

New SOc Waris: — L. Abrahiwnus 804: NSWAITGO:; Cobar, UN AHTE — Andros

wits NEWAITTO: Broken WIL TX ALK — Anes NSWAL7%3: Wileanila. VILLISST.

Wo Baterlow 0d; MEL: Tarella. VIlL1887, Jo kee Boorman. NSWAITTL: Comlobalin,

IN.L906. ~ CL Day can. MEL: Upper Darling biver, S78, — Holdings MBL: finetion at

Ninny and Darling Rivers. 1884, cho Marri (382); ADWLLIST, NSWATT74: Take’s

Grave, TON TH2O — G. Vo Sewnmedts BYR. Grillith, 28-V1TE 1927,

Vrevonta; — Anonying MIE: J pping. POY, P02, = Anew: MEL. Wo Acq. TRB

Nu, 752445; Mount Kosong. (14.N), WOR. Ankers MIL: Joparily OXI012, — ie Bi 19;

MEL: Like Boga, ucar Kerang, X.1803 — Sea te OAM @ MEL Black Rouge, Stawell.

PTS. -— J. PO Boeken dhe MELG Wimmera. 1890. — D. Keravhenbneht 29, ADBSO9054:

TAXONOMIC REVISION, GENUS MILLOTIA CASSINI 219

Field Naturalists’ Reserve, Dimboola, (t.N.1955, — F. Mueller: MEL: Grassland on the

Glenele (River), NI85L. — W, W, Watts 122) NSWITH9: Wedderburn Distr, X.1918,

— 1, B. Williamson: BRIOOIT7TE: Grunpiaw XLLG03, pp. — FT. Worsely: MEL: near

Jiake Hindmiwsh. 1&8,

Tasaranra: — Stuarts MMI: Tasman. p.p.

Scornann: — J. Fraser: & (photograph, drawings, and description of Kew specimen also

preserved in AD under ABOATZSON1, ADOAHAKOOL): Calafool, Galushiels, POVTI 108,

(tyme bb Millotia depauperata Stapl),

Disramurion anv Eeorocy

Occurs from the Shark Bay district of Western Australia south and vast

through that Stute, over the entire southern region of South Australia and north

through the Flinders Range and Olary Spur, through central and western

Victoria and southsyeslern and central New South Wales. There are also two

collections from Tasmania (Fig. 10-1),

The species grows primarily in sandy situations, but has been frequently

recorded in loamy and even hard rocky sandy soils; its habitat tolerance is

apparently the widest of any species of Millotia. lowering: September to

Sivas long the southern part of its range, and July to September (October)

in the north.

MORPHOLOGICAL VAKTATION

M. myosotidifolia is a rather polymorphie species, with greatest variability

in southavesf Arstralia. Variation is most marked in the habit and indumentum,

with specimens ranging between = glabrous erect plants with a central stem

leader and densely woolly or floccose ascending plants branched from the base,

Morcover, erect plints tend to be larger in all parts: compare the specimeus of

Anonym. Ll; ADIST24011; Rottnest, and Oldfield: W Acqn. 1859 No. 36953:

Murebison River, Tastern Australian plants are far more uniform. haying in

general an uscending habit and fairly dense woolly indomentnm as exemplified

by the specimens of D, Krachenhueht 29: AID95909054: Dimboola. Tepper

(275); AD935903122, MEL: from Clarendon is a peculiarly depauperate form

with + sessile flower heads,

The type specimens of M, glabra Stectz and M. robusta Steetz were col-

lected in south-west Australia; the former are typical of the glabrous, central

xtemmed forms of M. myosotidifolia, while the litter ure large specimens of the

woolly, basally branched forms. The type specimens of M, anyosotidifolla

actually fall between these extremes. Although Sonder (1853) treated ML, glabra

ond M, robusta as varieties of M. myosoticlifolia, variation between them is su

continugus that they cannot be distinguished,

M. depauperata Stapf is clearly a depauperate specimon of M. myosotici-

folia — Fig, 9, D. Ina footnote to the type description. Stapt says Lhiul the

“species” was “na doubt accidentally introduced from Australia’. Tt is riost

likely that seeds of Af, myosalktifolia were introduced at Galashiels, which is

womilling centre for wool, from an Austiutlian wool clip. G. L. Davis (1952)

his also recorded the introdnetion of Calotis squamigera. C. T, White at Gala-

shiels which doubtless oceurred through similar circumstances.

2. Millotia greevesii F, -v. Muell., Mragm. 3(1862)18, t.18; Benth, Fl Austral

3( 1867 )596; Tate, Trans, Roy, Soe, §, Anstral. 3(1880)72 ?p.p.. Fv. Muell,,

Svst. Gens. Austral. Pl. (1882)52; Moure, Cens. Pl. N.S. Wales (1584)37,

F, y. Muell., Sec. Syst. Cens. Austral. Pl. (1889)139; Tate, ‘Trans, Roy, Soc.

22 BK. sCHODDE

S. Austral. 12(1889)100 ?p.p.; Bailey, Cat. Pl Queensl. (1890)23; Tate,

Handb, Fl. Extratrop. S$. Austral. (1890) 119, 239 ?p.p.; Moore & Betche,

Handb, Fl. 8.8, Wales (1893)286; Bailey, Queensl, Fl, 3(1900)843; Dixon,

Pl, N.S. Wales (1906)197; Bail, Compreh. Cat. Queensl, Pl, (1913)267;

Sulman, Guide Wildfl, N.S. Wales 2(1914)83; Maid, & Betche, Gens. N.S.

Wules Pl, (1916)201; Black, Fl, S$. Austral. (1929)638 p.p.; Black, Fi. 5.

Austral. ed. 2, (1957)917 p.p.

Tyveu: H. Beckler : K: Barrier Ranges.

The Kew specimen, possibly the only one extant and therefore the holotype.

was scen from a photograph in CANB (Neg. No, Kew 1637, 10.19.1953)-

Grey herb, sometimes virescent when young, (2)3-15(20) cm tall,

(2)3-20(30) em broad, Jndumentum dense white lanuginose, with golden

glandular pilose hairs intermingled on upper stems, upper leaves, peduncles and

involucres in some forms. Stems (2)4-15(50), ascending or decumbent, slender.

Catyledons (4)5-6(7) mm long, Leaves narrow linear to + filiform, (44)%-2

(2'2) em long, hardly amplexicaul, becoming progressively shorter up the stem

fyom the base. Flower heads (1)5-100(300), Peduneles less than 1 em Jong

and indistinct to 1-8 em long and distinct. Involucres 4-6 mm long, of 7-1

uniseriate rarely * biseriute slightly imbricate linear bracts with navicular mid-

ribs 1-3 x as broad us the straw-coloured margins and acute + fimbriate apices,

Flower heads with ca. 10-100 Horets, Corollas funnel form, 2-3(3'%) mm long,

deflexed over involucre (peripheral corollas most deflexed), bright yellow, with

the tube sometimes becoming reddish after anthesis; corolla limbs of 5 fully

spreading acute lobes 4-44 mm long. Stamens 5, with tips prominently exserted

beyand corolla limb; anthers with oblong thecae (¥)%%-4(1) mm long, the con-

nective tip extending 45-75 mm _bevond the theca; pollen grain diameter (15) 18-20

(22) mw. Style branches 1-140 mm Jong, with acute broadly dilated conical

uppendages at the apices. Cypselae papillate, linear to filiform, 3'-8 mm long,

with central cypselae of head protruding to 3 mm above top of involucre and

peripheral cypselae rarely longer than involuere, bruwnish to reddish black, the

heak usually paler; cypsela papillae rather dense, obtuse, often larger on beak.

brownish slightly transparent; cypsele beaks #244 mm long, slightly compressed

and distinctly demarcated. Pdppus various, of ca (5)10-20 plumuse setue =

“i length of corolla, or of predoutinantly minute scales with rare solitary setuc,

or absent.

Disrrisution AND EooLocy

Occurs through the south-central arid region of Australia, confined to sandy

hiwhitats which are so widespread through its iusrea of accwrence that its dis-

Wibution is + continuous (Fig. 10-2).

subsp. greevesiz

_ Habit decumbent to_ascending. Involucres 5-5!6(6) mm long, Cypselae

(4+)5-7(8) mm long; beaks (1)2-4(5) mm long; central cypselae of head pyro-

truding (14)1-236(3) mm above top of involucre, with surrounding cypseclac

becoming progressively shorter to the peripheral eypselae which protrude up to

L mm above top of involucre or not at all, Pappus of ea. (5)10-20 plumose setac,

%4-1'4 nm Jong.

DistRIBUTION

Confined ta the region east of the Finke River (Central Australia) and

Flinders Range (South Anstralia) to the arid plains of south-west Queensland

und central New South Wales.

“Ww

[Fe

Fig, 2. Millotia greevesii FP, v. Muell, yas. greevesti. A, whole plant (Cleland; AD

95730073): B, involuctal bract (Cleland: AD95730073); CG, Hower head just after antlussis

(Cleland; AD95730073); D1. mature onter floret af Hower hewl, D2, mature inner floret

of Hower head, D3, floret showing slight reduction of pappus (Cleland: AD95730073); E,

mature cypsclae showing stages of reduction of pappus (Menzel 45); F, whole style and

androccium (Cleland: AD95730073).

3223 R. SCHODDE

var. greevesii

Habit + decumbent, but often ascending, {2)4-7(10) om tall, (2)5-20

(32) em broad. Pedincles indistinct, varcly 4+- 1 om long, with cauline leaves

(of decreasing Jength) right up to flower head. Involucres grey-white, the (7)

8-9(12) bracts covered with a dense white lanuginous indumentum which

binds them into a seemingly commate involucre. MWeads with (10)15-25(33)

furets. Central cypselae of head (5'2)6-7(8) mm long, beaks (244 )2%s-34/ 4)

mm long; peripheral cypseluc. (4)4%-5'2(6) mm long, beaks (1)T4-24(2':)

mm long. Papprs of ca, (5)10-15(20) plumose setae which are sometimes con-

spicuously unequal in length {due to reduction) (Fig, 2).

Svecimens ExaAxuNen

Sout AuscAmma, — Anonym. (Herb, J. M, Black): AD95911087: Yadlakeena

(= Yaclakina Well). — J.B. Cleland: AID95730073: Willitum Crees, 18.VIIT1930, 10.1X.1930.

Herb. O. E, Menzel 45: AD95724020: ITereott Springs (= Marrev). 1895, — T. GC, &.

Ovsborn: ADO5724052; Curnamona. 24.VIL.1923.

QureNsnAnp; — Wheeler: MEL: Between Stukes Range und Coupers Creck,

New Soutw Waurs: — Anonym. 38 (Herb. J, GC, O, Tepper 2046); AD95833148:

Culpaulin, VILES93, — Avenyne: Wo Acqn. 1889 No, Thr. Barrier Ranges. (part

of type?). — Anonym, 445 MEL: Mombasa. Mount Murchison. — W. Bduerlen 221: MEL:

Koontngbicry (= hoorninugbirry ), UX.1887, — N.C. Beadle; SYD: Near Pooucarie, VIT.1042.

Distreutioy AND Ecowocy

Lake Fyre Basin and north and eastern margins of Flinders Range east and

south ta the Paroo and Darling Rivers (Fig. 10-2). Plowering: July-September

| December).

var, glandulosa Schodde, var. uov.

Affinis var, greevesii, sed habitu altiore ercctioreque (etsi semper a basi

ramoso), pedunculis distinetis (1)2-5(5) cm longis sine foliis caulinis. numero

maiore (7)10-15(18) bractearum involucralium, numero maiore (30)50-60

(80) florum per capitulum, ct praccipue pilis glandulosis super bracteae in-

yolucrales, pedunculi, folia superaque, differt.

Typus; W. MacGillivray 1002: ADW s.n., BRIO0S770 (hololypus); Near Ada-

vale. 28. VIET.1923.

Habit ascending, more upright thi var. greevesti (3)9-15(17) env tall.

Peduncles distinct, (1)2-5(8) em long, densely white woolly or predominantly

golden glandular hairy under the Hower heads, without cauline leaves but

often with several vires¢ent, glandular hairy peduncle leaves c. 2-5 mm long.

Involucres. virescent, the (7)10-15(18) bracts free with midribs golden glan-

dular hairy and dense to sparse (rarely absent) white woolly hairs on margins

of midribs, Heads with (30)50-60(80) florets. Central cypselag of head (52)

6-78(8) mm long, beaks (3)38-44(5) mm long; peripheral eypselae (3 )4-54(6)

mm long, beaks (1)2-3(3%) mm lung, Puppes of (10)13-17(20) plumose sctae

of + equal length (Fig. 3),

The golden glandular haired involucre is the principal character distin-

suishing this variety. The only previous reference to it has been made by

Mueller and Tate (1896) when describiny Millotia kempei var, helmsii.

——e

sag

rae

——

wasps PS

ran

ere ee es pth

meee ayers es me ta Pe Tt

Wie. 3. Millotia greevesti var. glandulosa Schodde, A, whole plaut (type—MaeGillivray

and glandular indumentum intermediate between var, greevesit and yar. glandulosa (Betche:

AD95727059), D, flower head with florets maturing after anthesis (ty e—MacGilhvray 1002);

EL, mature outer Horet of Hower head, E2, mature inner floret of flower head (type—Mae-

Gillivray 1002); FL whole style and androechue (typo—MacGillivray 1002).

234 RK. SCHODDE

SeuCIMENS EXAMINED

Queenscanp: — Bueknell; NSW41763: Hungerford. UX.1910, — §. 0. Everist 1648:

BRIN04768; Gilruth Plains, near Cunnamulla. 17.0X.1958. — W. MacGillivray 1002: ADW

s.m., BRIQUATTO: New Adiavale. 28.VI1I.19233. (type). — J. Wend 698: BRIO04T69: St.

George, X.1894.

_. New sour Wares — E. Betche: ADY5727059 ex NSW41764A: Paroo River District,

IX.1900. ~— J. T. Waterhouse: AD95922010; Invernay (near Collarenebri}, 24.04.1951. —

W. Campbell: NSW41764B: Bourke, 117.1893.

DistRiBUTION AND ECoLocy

East and north of the Paroo River (New South Wales) to St. George and

Adavale (Queensland) (Fig. 10-2). Flowering: August to October, with one

record in March,

subsp, kempei (F. vy. Muell,) Schodde, comb, ct stat, nov.

Millotia kempei F. v. Muell., South Sci. Rec, 2(1882)2; F, v. Muell., Syst.

Cens. Austral, Pl, (1882)82; ‘Tate, Trans. Roy. Sve, S$, Austral, 5(1882)87;

F. v, Muell., Sec. Syst. Cens. Austral. P. (1859)138; Tate, Trans, Roy. Svc;

§. Austral. 12(1859)100; Tate, Handb. Fl. Extratrop. $. Austral. (1890)119,

239; Tate, Rep. Horn Exped. 3(1896)166; Gardner, Enum. Pl. Austral, Occ,

(1931 )134,

Type: H, Kempe (238); MEL (lectolype), NSW41759: (Prope) Finke River.

TX.1880.

Habit ascending, very rarely decumbent or erect. Involucres (34 )4-5(6)

mm long, Cypselae (3%)3%-5(68) mm long, beaks (#)4-14(24) mm long;

central cypselae of head + equal in length to involucre, the beaks rarely protrud-

ing up to 1 mm above it, peripheral cypselae little shorter than central cypselue

and exceptionally longer than involucre. Pappus absent, ar of predominantly

minute scales with rare. plumose setae ca. 4-1 num long.

DistrisuTion

Confined to the region west of the Finke River and northern Flinders Range

to the Nullarbor Plain and Victoria Desert (Western Austrulia).

yar, kempei

Habit ascending, rarely + decumbent. Peduncles + indistinct, rarely up

to 2 em Jong, often with cauline leaves (of decreasing length) right up to

flower head. Involucres grey-white, 44-6 mm long, the (7)9-12(15) bracts

covered with a white lanuginose indumentum which may bind them into a

scemingly connate involucre. Heads with ca, 20-30 florets. Cypselne 4-64 mm

long, beaks ca. 3-2% mm long, Pappus of minute scales and rare plumose setae,

more rarely entirely absent (Fig. 4).

Specimens EXAMINED

Crentran Austraua! — 1. Kempe (238); MEL, NSW4L7S59: (Prope) Finke River.

TX.18S80, (dype of Millotia kempei F. v. Mnell. ).

Sourmn AvustTRAnia: — Anonym. 14: MEL: Peake. — Herb. O. E. Menzel 45:

AD95724020; Hergott Springs (= Marree). 1895.

225

ASSINI

ene

a ete

eee

Gis

Nuss &

228

SFL

wv Pin

Be ot

3 Ge

af ost

Age

DAR

Born

£584

ser

re us

a He

<+12e

“BUE

+S oo

go aw

Zo!

SEER

Seo y

vune

mad —

aa]

Ts 2

mOUBE

cae

Faqs

in 4

ae a

Pane

enti a

Sin.

Ste rd

Aes

320

aR ye

eit &

reg a

o ..

=.% os

aM a5

>| o.2

2 ede

B pe

Ser for

sibs

Sau Gen

Seas

wi~

= =

Hee

ory

bs nd =

ad oy

ary

Fig. 4.

> B, involuecral bra

reduction (Menzel 4

rudiment.

45)

236 R. SCHODDE

DistRIBUTION AND ECOLocy

Found along the western margins of the Lake Eyre Basin, between the

Finke River and north-west Flinders Range (Tig. 10.2). Flowering: September,

Rare in herbaria, the aboye cited collections comprising the only specimens

seen,

yar, helmsii (Tv. Muell, & Tate) Schodde, comb. nov,

Millotia kempeit var. helmsii F. v. Muell. & Tate, Trans. Roy. Soc. 5, Austral.

16(1896)368; Black, Trans. Roy. Soc. S, Austral. 43(1919)43; Black, Pl. S.

Austral, (1929)638, pl. 51( 1-2); Bluck, Fl, S. Austral. ed, 2, (1957)917,

f, L197(1-2).

Toxanthes whitei Black, Trans. Roy. Soc. §. Austral. 39(1913)840, pl. 69.

“Toxanthus whitei”.

Tyree: R, Helms; AD95731002, A1D95732063, MEL (lectotype and ixolectotype ).

NSW41761: Between Birksgate and Blyth Ranges (Camp 22, Elder Ex-

ploring Expedition), 16.VIL1891.

Hahit useending, exceptionally erect, Peduncles + distinct, 2-5 cm long,

golden glandular and white woolly hairy, usnally with several glandular hairy

peduncle leaves which grade in increasing length into the cauline Jeaves below.

Incolucres virescent, ca. 4-5 min long, the (10)12-16(18) bracts free with

midribs golden glandular hairv aud dense to absent white woolly hairs on

margins of midribs. Heads with (20)30-70(100) Horets. Cypselae 3-52 min,

beaks ea. B-1mm long. Pappus absent, exceptionally with rare scales or plumose

sclae present (Fig, 5).

SPECIMENS Exaxunrou

Westexrs Ausrnataa: — BR. Helms: AD95731003: Vitoria Desert (Camp 54, Mider

Exploring Expedition), 171%, 1891.

CenrraL Avstrata: — fl. Based: BRIOOATTL, NSW41762, PERT sav: Finke

River District (5. Austrdian Medical Relief Expedition). 1919. — R. Sehudde 390;

AD95807233: Central west base of Ayers Hock, S0OVITL.1997_

Soctu Ausimania: — Anonym. (Herb. RB. Tate): AD9S9INO47: Tdyaka sandhills,

21X.1883. — J. B. Cleland; ADS5730071; Oalden Soak. 20.VILL1939. — It Heli:

AD95731002, 4195732063. MEL (2 sheets), NSW41761: Between Birksyate and Blyth

faners (Camp 22, Elder Exploriny Espeditiun), 1G.VITASO1 (type of Millotia Kempei var.

helmsii F. v. Muell. & Tate). — T. RB, N. Lothian L/768a/54: AD95918015: Rock lale, De

Hose Will Stadion. G.VTI1954, -- D. J, B. Whibley 680; AD96051015; Maralinga—Suni-

hills Rifle Range — ca. 55 kny north of Watson. 16.1N.1960, — 8. A. White 107 Cferh. J, M.

Black): ADY5731004; Claypan between Wlat Rock Hole and Morrilyanna («= Monarilyanna)

Native Well. 26.VIL1914 (holotype of Trxanthes whitei Black), — 5. A. White, 1, 3 4:

AlD95833147, MEL, NSWAITG60; Everard Range. S.VULI9I4 (paratgpe of Toxenthes

white: Black). — PF. -G. Wilson 1840- ADOGISOL0G: ea. 32 km cast oF Ooldea, 24,1N,1960.

Distatpurian Ann Econocy

From the Finke River and northern Flinders Range south and west to the

Nullarbor Plain and Victoria Desert (Pig. 10-2), Flowering: July to September,

Aboriginal name: “Tjudernra” (Ooldea, fide J. B. Cleland).

Black published Voxunthus white’ in ignarance of Millotia kempei var,

helmsii F. y, Muell, & ‘Tate, an oversight he himself later realized and corrected

(1919).

owe

Ce af

}

aa:

bY ‘7

he 4

ie Be

Vek i

ui 3

Lat

bag, 5.

showing presence of rudimentary pappus in varying degrees (Lothian L/76$a/54); GC,

whole style and androccium just after anthesis (Wilson 1818),

225 K. SCHODDE

Morexococican Variation in Millotia greevesii

Variation in the pappus, a character normally so stable in the species of

Compusitae, is undoubtedly a most striking feature of this species and has led

\fueller (1852) and later authors to distingnish the apappose forms as a distitiet

spevies, M. kempei, Other characters showing change are the habit, involucral

indumentum, and the length of the cypselae beaks.

All variations are elinal, giving rise to the following patterns,

({) in the pappus: Along the western margins of the Luke Eyre basin there

fs a relatively sudden transition from the fully pappose forms of the east to the

apappose forms of the west. Specimens in the collection of O. &. Menzel 45

from Hergott Springs (AD95724020) show various stages in the redaction of

pappus, and type material of M. kempei, hom farther north, possesses a rudi-

inentary pappus’ of scales and occasional solitary setae, contrary to Mueller's

original description, All traces of pappus are absent in specimens of the vlan-

dular-haired var. iclmsii except in two eusterly collections — 8, A. While 4:

MEL; Everard Ranye and T. R.N, Lothlan L/768a/54: ADIBMISOLS: De Rose

Hill Station — in which the pappus is of seales;

(2) inthe cypselac beaks; From east and north-east to west aud south-west,

there fs a Seatttiak teductian in the length of the eypselac beaks. Significantly,

it becomes most marked along the western margins of the Lake Eyre basin, and

tovether with the change in pappus provides the basis for separating the twa

sub-species, grecvesit and kemper;

(3) in the involucral indumentum: Forms in the east and north-east, and

in the west and south-west areas have glandular-haired involneres; those in the

central area, which have woolly-haired involucres, grade on either side inta the

vlandular-haired formas, Examples of intermediates are from the Paro River

District (B, Betche: AD95727059) on the east, and Everard Range (S$. A. White

1, 3, 4; AD95833147, MEL, NSW41760), De Rose TIill Station (7. A. N, Lothian

L/768a/54: A1D95948015), and Ayers Rock (A. Sehodde 890: AD95507233) on

the west. Forms with woolly involucres possess fewer Horets per head, The

two glundular-haired groups are distinguished as distinct vurieties:

(4) in the habit: There is x gradual north to south change from an ascending,

to a + decumbent habit iu those centrally located forms of AL. greevesii with

woolly involueres. Both glandulur-haired yarieties possess a cousistently aseeud-

ing abit,

3. Millotia macrocarpa Schodde, sp, nev.

Millotia greevesti (non F. vy, Muell.) Tate, Trans, Roy, Soc. S, Austral

3(1880}72 2p.p.; Tate, Trans. Hoy. Soc, $. Austral, 12(1889) L00 °p.ps Pate,

Handb. Fl. Extratrop. §. Austrah (1890)119, 239 Yp.p.. Black, Fl §. Austral.

(1929)638 p.p., Black, FL S. Austral. ed. 2, (1957)917 p.p.

Annue incana, 2-8 em alla. Indwientum conterte lanuginosum, sine pilis

whindulosis. Caules agcendentes diflusi, vel interdim ereeti neque a basi samosi.

Cotyledonvs 5-7 mra longae. Folie anguste lincaria, 2 em longa, vix amplexi-

vaulia, Bracteae involnerales 6-9, lincares, 64-8% mm longae, sine cacuminibus

rubidis: costae mediae bractearum naviculares, conferte lanewe. -- 2 4 milrgines

seariosue ubdite Jatitudine. Flores 15-25 raro plures per capitulum. Corolle

anguste evathiformes, 2-2 mm lungue, + defexue, tribus vel interdum quattuor

lobis paene obtusis, + leviter expanditis sed interdum erectis, + 40 mm Joneis,

TAXONOMIC REVISION, GENUS MILLOTIA CASSINI 229

Antherae theeae cllipticac, + 0-4 mm longae, Styli ramt & ¥ mm longi, apice

acuti et leviter dilatati, Cypsélae muricatae filiformes, umnino rubidae, (th

10(12) mm Jongae, et (1)2-3(4) mm supra involuero extensac; rostra ey pyse-

forum 38-74 mm Jonga, leviter compressa, Pappiselae semi-plumosae, erect

vel leviter expanditae, 4-4 x corollae Jongitudine,

Affinis M. tenuifoliae, sed habitu, indumento eglanduloso, corolla deflesa

valde triluhata, Jongitudine cypsekuwum. et pappi setis semi-plumosis erectiori-

busque pracsertim differt,

‘Pypus: PLC, Wilson 596: AD95903126 (holotypus): North Gawler Range, south-

west of Lake Gairdner. 13 km south of Mounaree Head Station, near the

main road between Moonaree HLS, and the Nonming-Yardea road. Growing

in reddish sand, 16,X.1958.

Grey herb. 2-8 em tall. Indumentum dense white lanuginose only. Stems

1-10, usnally ascending, rarely simple or erect, slender. Cotyledons 5-7 min lone,

Leaves marrow linear, +2 em long, hardly amplexicaul, becoming progressively

shivter up the stem from the base. Flower heads (1)2-15(30), on short

peduncles up to 14 em Jong. dnvolucres 64-84 mm long, of 6-9 nniscriate near

Hracts. with lanate nayicular midrihs + 2 x as broad as the concealed straw-

coloured margins and acute finely fimbriate apices. Plower heads with oa. 15-25

florets, slightly honey-seented. Corellas. uarrow cyathiform, 2-24 mm long,

slightly deflexed over involucre (especially the peripheral corollas), cream,

with the fube often becoming dark reddish-parple after anthesis; corolla limbs

of 3, sometimes 4, = obtuse slightly expandod lobes ca. “oe mm long, Stamens

3-4, sometimes 4 in a 3-lobed corolla, almost entirely enclosed; anthers with

elliptic thecae = 25 mm Jong. the conwetive tip extending {i mm beyond the

theea; pollen grain diameter (17 )22-25(28) x. Style branches % mm long, with

nurow obtuse, slighUy diluted apices. Cypselae muricate, filiform, rs 2)

mim jong, prtruding (1)2-3(4) mm above top of invalucre, entirely reddish-

black, rather densely and eveuly covered with slightly transparent papillae which

are identical tr shape with those of MI. tenmifolia and larger on the beak: eyparele

leaks 347 rom long, slightly compressed and distinctly demarcated. Pappns

of ca. (12)15-20(25) erect or slightly spreading semi-plumose setae 4-X length

of corolla (Fig. 6).

Svccmiuns Exascmin

Sorte Auyinaniar — Anouym, (Herb, A, Yate): AD95734022: Blanchetown, VITT.1&S 1.

» Anonym. (Herb, R. Tate): A095724029. MEL: Vadlacena (= Yadlakina) Soakage, Lake

Torrens Pliin. 18.VITLI883, — 1.0.8.0, (— 1..G, B, Osborn); ATI95731022: Koonuniore.

27 VITT 1923, —_ 2. G. Wilson 536: ADIS90R128: Gawler Range. 2 kin west of Peterby

Tank. 16.4.1058, — Po G. Wilson S96: ADIS9N3I26: North Gawler Ranve, south-west of

Lake Gairduer, 13 kiy south of Moonaree Head Station, I8.X.1058 (type).

Vieyouta: — A, C. Beanglehale 1098: Merb. Beauglehole: Kulkyine National Bonest

X,1645.

DistTeiBpetion AnD Meonocy

Althongh it is rarely represented in herbarium collections, Mf, macrecurpa

apparently oceurs through the seii-arid parts of South Australia from_ the

Gawler Range. around the margins of the Vlinders Range to ihe northern

Murray Mallee, and extending into north-west Victoria, Ceographically, it

overlaps the distribution of all other species of Millotia (Fig. 11-3).

Grows in open red sandy situations, Flowering: August to October (not

Jiuter ).

B, in-

ead at anthesis (Tate

and androveium (type—

ftype—Wilson 596);

lant (typ

flower h

6); €

A, whole pl

( type—Wilson :

: D, mature florets (type—Wilson 596); E, whole style

ya Sehodde.

hives

Millotia amucrocar

29 )

, &.

volucral bract from mature inves

Wilson 596).

Fis

ADY57240)

TAXONOMIC REVISION, GENUS MILLOTIA CASSINI pars 9

Morpua.ocscal, Varta'vion

Liven though the series exumined is ton sinall ta permit generalisations ure

Variability, specimens in extant collections, which are from widely separated

localities, are notably uniform in all parts.

4. Millotia tenuifolia Cass., Ann, Sci, Nat. 17(1829)31, 417; Cass., Dict. Sui. Nat.

60( 1830992, DC. Prodr. 6(1538 )161, Steetz in Lehm., Pl. Preiss. 1( 1945

456; Walp. Rep. 6( 1846-7294; Sonder, Linnaea 23(1653)502, Ilannaford,

Notes FL & Faun, Vict. (1836)61; Mook. £, Fl. Tasm. 1(1856)209 p.p..

Benth., Fl, Austeal, 3( 1867 )396 p.p.. Jolmston, Memorand. Tusm. Botanists

(1874)24 "pp, Spicer, andh. Pl. Tusm. (1878)27, 117 py; F. v, Muell.,

Trans. Ruy. Soe. Tasm., Rep. for 1878(1879) 17 pp; Tate, Trans. Roy. Soc.

S, Austral, 3(1880)72 pp. I vy. Muell,, Syst. Gens. Austral. Pl (1882)82

tep.; Moore, Cens, PL N.S. Wales (1854)37 pips F. v. Muell., Key Syst.

Viet. Pl. 2(1883)34 pps bev. Muell., ibid, (1887-8)337 pp. F. v. Muell..

Sev. Syst. Gens, Austral. Pl, 1(1889)138 p.p.; Tate, Handh. Fl. Extratrop.

8. Anstral, (1890)119, 239 p.p.; Moore & Betche, Handb, FI, N.S. Wales

(1893) 256 p.p.; Rodway, Tasm. Fl. (1903)54 Ppop.: Dicls & Pritzel, Fragm.

Phytograph. Austral. occ, (1905)616 ?p.p.. Dixon, Pl. N.S, Wales (1906) L97

pps Sulman, Guide Wildil, N.S. Wales Z(L914)83 ?p.p.; Maid. & Betche,

Cens. N.S, Wales Pl, (1916)20L p.p. PVN. Clu Viet. Cens. Pl. Viet. (1923)

67 p.p; Cleland & Black, Trans. Roy. Sov. S. Austral. 51(1927)59 p.p.;

Black. Fl. S. Austral. (1929)638, £291 p.p,; Ewart, PL. Viet, (19381)1139

p.p.; Gardner, Enum. Pl, Austral, Occ. (1931)134 ?p.p.; Black, Fl S. Austral.

ed. 2, (1957)917, £1215 p.p.

Alillatia Rispidule Gandoger, Bull. Soc. Bot, France 65(1918)45; Cardner,

Enum, PI, Austral, Qee, (1931) 134

Tyrr: D'Urville; P (feetotype): Port du Roi George (= King George Sound}.

Virescent herb, becoming greyish only = after seed maturation, (36)2-10

(14) cm tall, Vegetative parts with uromatic odour, Indwnentum of white

woolly and pale golden glandular-pilose hairs, the latter most prominent om

young parts and Jonger than those of M. greevesii, Stems 1-6(20), erect and

branched from near the base, rarely ascending or simple, slendor, Cofylecdons

2-5 (6) mm long, often strongly reeurved. Leaves narrow linear to linear, excep-

timally becoming oblanceolate, (42)%2(2k) em Jong, 1-3(5) mm broad (itt

the widest part), hardly amplexicaul, relatively dense. Mlower heads 1-15

(+100). Peduncles (4)1-4(8) em long raising the involucre (0)%-3(8) cm

abiove the tops of cauline leaves, + slender. Involneres sete rity lions,

of (5)8-14(20) + uniseriate hardly imbricate linear to oblong bracts with

navicnlar midribs = 1-3 x as broad as the straw-coloured rarely red-tinted

margins; bract apices acute to attenuate, fimbrinte, sometimes red-purple, Plawer

heads with ca, (5)L0-40(65) florets, Corollas tubular, (14 2494) mm lone,

+ erect, rarely deflexed, lemon yellow (?white in Tasmania), with the tube

becoming deep purplish-red after anthesis, corella links of 4 (exceptionally (

or 5) + erect narrow obtuse lobes (%)%-ho(#) mm long. Stamens 4 (excep-

tionally 3 or 5), = entirely enclosed; anthers with elliptic theeae ('5)%403%(%)

mm Jong, the connective fip extending (40)%-M('4o) mm beyond the theca;

pollen grain diameter 20-25 yp, Style branches (2)%-%(1) mim long, with narrow

oiytiuse hardly dilated apices, Cypselac muricate, linear-clavate, (3)4-6( 7H)

mm long, the upices + level with top of involuere, reddish-brown to reddish-

black, the beak often conspicuously paler, cypsela papillae + dense, evenly dis-

peasintiindetiesy

he Sea wes -

Sarna die ae

act

eS So ae

Hig, 7.

involucral bract (type—D’'Uryille; P): C, flower head with maturing cypselae (Schodde ee

D. forets with maturing ecypselue (1 = Schodde 1015, and 2= Schadde 932); E, whole style

and androeciam (Schodde 932).

Millotia tenuifolia Cass. var. tenuifoliz, A, whole plant (Schodde 932); B

TAXONOMIC RiEVISLON, GENUS AMLLOTIA CASSINI 233

Wibuted over cypsela, + acute conical, + larger on beak, trausparent to whitish

translucent; cypwela becks (4)1%-24(38) mim low, not compressed, meruins

dradually into ovular region, Pappus of (19)20-30(35) + ascending spreading

fine barbate setae which are + slightly longer than corolla and evenly and

relatively sparingly toothed to the apices, and rarely shorter or reduced to seules-

Distimurios 4anp EcoLocy

Oecurs in the south-west of Westerte Australia cast to Esperance, and in

south-eastern Australia from Eyre Peninsula and the Flinders Range south and

eas) through the southern Murray Mallee, aeross central and southern Victoria

tu the Australian Alps and west Gippsland. Fairly widespread in) Tasniania.

Cardner’s collection from Wihina is anomalous (lig. 11-4),

Grows in uw moister habitat than any other speeics of Millotia, on infertile

erey rarely reddish sands— ulthough ocewsionally recorded om clayey or stony

Jeached soils —and is generally associated with a heathy or selerophyllaus

vegetation, Flowering: September to December,

var. tenuifolia

Herh (%)3-10¢14) em tall with 1-15 (+ LOO) flower heads. + erect corullas

and puppus setae + as Jony as or slightly longer than corolla (Pig. 7),

Sueucimens ExAminiin

Westen AvstHantar — Anonyme: Ps Part-du Not Georges (= King George Sonn), —

Brooke: MEL: Nour tsrachite Bay. XUILISSt o- N. TT. Burbidge 2379; BRIOOATT3, CANE

14453) Badjaming Hill, west of Weagin, TO IN,1947 - Dempster: MEL: Between Msper-

ance Tay & Traser’s Aange. 76. — D'Urnille: Py Port du Roi George (- King George

Somd) Crype of M. ternuifolia Guas,). — A Baton; MEL (2 sheets); E.. (= east) of York,

1889. pop. — Hy, Fiehler 16798: ADVBNN9NAS: Cu. JOR hin south-east of Donnybrook, wear

Nowhuidls, 3 1N,1959, — W. V) Fitegerakl: NSW4ITSS: Boulder. INTS895. pop. — €. A.

Gardner B 369, 560. PERTH sane 2Neur Wilunw VINTOSE. pp — Neal; MUBL: F,

(= east) saurees af Swan Rivier) 7889, py, — MVerrall; Mika Vilgnrn. Taa8.- AL Mor

ris, LY: Kelmscott, Cunning River. LOAXIS98. pop. (type of AL, fispidula Gder,), —

Preiss 68; HBG, MEL (2 sheets), 2, W. Aco. 1880 No. 1380457, Woon. Melville OG.

Plantwwenct, (Swan River Colony), O.X.84 — A, 2. Reyes 1207: PERTIT T, 1600/44:

® milous east of Thallicht. Q4N.1946. pup.

Soorm Augmmace: — H.W.A, (= A, W. Andreu): AD95731026; Ashbourne, A.TN.1919,

— Anonyine (Werb, J. MW Black): ADDSTB1020; Beettloy. AUL1908, qup. — Anongon. Céferk’,

JOM. Black): AD95731023; Karbondu, 58,1915, pup, — s\nenyn, (Werh. Ry Tate):

ADSS72400d; Wirrabara. X.1883, — A. Barton: Al95807068; 2 wills north-east of Vietar

Harbour, L3X,1957, - Ui Biehler 1276868: ADQASTITOOL: Gammon Ranges North Tusk,

J918, 1956. — Wh, Biehler 13947, AD9S5T50023: Southern Yorke Peninsula, Gi. 8 kan south

of Corny Point 25.08.1957. — EB. H, Ising 1080; ND9SS)TOT5: Moolooloo Station, N.1918,

— Bal. bing on; ADISSITN20; Warren Reservoir, TON1023, - 2. I Tsing: Since Al

H5SL7OL3; Crafers, WN TU80, — OB. A, Deine sane: ADSSRLT009; Arno Bayo 27.WIT1996.

i, WE, Using aaa ADO5833163; Gawler Kee, (— ange). 13.17.1938 — Fy IP. feng ane:

AD95833163: Mt. Waclinna. 29.0K.1939. Cl. WW. Jolins 4: ADSSTSIOLO: Wadinns. pa. —

Bb. Myeflerrs MEL, Bale Range. Tolly Ranges. S.TR48. pop. — RR. Beha S03. AD

H5b07169: Ca. lL han north-west of Gawler, 298.1957, — A, Schade 509: ATDOSKOUTONS >

Golden Grove. en. 16 kin northecast of Adelaide. 5.X.L857. — R. Schodde 91d; ADPSHU8093:

Bast side of Chauncey'’s Sine-Monato South road, ca, 8-1 kar north of the junction of

Chaonceey’s Line ancl the Chauncey’s Line-Monarto South toul., 4.X.1058. — HK. Schodde

932, ADOSIN8N82; Ca, 2 kin nerth of the junction of Ghannaey’s Ling and the Monarto South

to Ghauneey’s Line road, 4X P958, pp — KL, Soeeht; AD: Dark Tsland TTeath, 10 miles

NNE (of) Reith IN.1952. DO. Job. Whihley 888: ADYS9Q00IHG: Marble Rayse, 7 sniles

along Warrow-Melillitie road. 10.X.1958. — EL. 2. Willams 8: ADI5909030: Meningie.

7A L958, — POG. Wilson Of: ALYS9NV0NS: Whyalla-Gowell road, co. 47 kin south of Whyalla,

LX.1988. — PF. GL Wilson TA7: ADYSANG0K6s Whyalla-Kimba road, ¢.. 74 kin awyest of

244 RK. SCHODDE

Whyalla, 3.X.1958. — P. CG. Wilson 333h: AD95915022: Stumford Hill, c. 8 kin south-east

ol Port Lincoln, §.X.1958. — BF. G. Wilsow 506; AD9S90909T: Gawler Ranges; Yandinge

Hulls, c. 32 kin north of Minnipa. 16.X.1958 — P. G. Wilson 892; ADYS908171; Kangaroo

Idand. Near Birehmore at ee 21 kin south-west of Kingsente. 12X0.1958. — PL G,

Wilson 2126; AD9620L145: Ca. 97 km north of Bordertown on Pirinaron-Bordertown road.

SOVITI961. pep.

New Sourm Waxes: — Anonym: MEL: Near base af Mi. Kosciusko, X.1S87, — BE. J,

MeBuarron 1996 (biy): NSWALTGS: Monument Will, Albury, 12.TX.1948.

Vieronta: — Anonym, (FF. Mueller): MEL: Seymour. —- W.R. Baker; MBL; Jeparit.

OM19L2. — AL W~ Brotherton: MEL; Laddon River; 1894, — G. Freneh: MIL, (2 sheets):

NW, (= north west) of Lake Albacntya. EX.1887, — GC. French jr: MEL: New Dandenong

Crock. 1892. ~ C, Green SY: MEL: Aracut Plains. ~ D. Sullivan 39: MEL: Moyston.

- a B, Williamson sz BRIOM776; Grampians, NL1903, pip. — W, B. Wilson 5: MEL

(2 sheets): Near Geeloum. 1885.

Tasarania: — E, Atkinson 147: WO 1450 5: Enon road. 14.X1. aa — J. Buflan 27:

MEL: Port Arthur, (892, — A. V, Giblin: HO H450 3; CG. (= Prony J ake, — A. GC. Gunn

164. HO HA50 1, NSW41806, NSW41807: Epping Forest. 17.4,1542, Glen Leith.

24 248 TBA). 1833. — J. Milligan 1086: 11O 450 2, MEL (2 sheets), NSW41808: Killi(e)-

crankie-Flinders Island. 4.X,1847, — L. Rodway: "NSWdAl809: Near St [le iso's Teuds.

1X.1892, — FE, Redtway: CANB8636, HO H4507: Mt, Fa(u)ikener, X,.T922. A. Sonyycne;

BRIOOIT75. Near Launceston,

Distrinurion AND EcoLocy

Distribution and ecology as for the species.

vat, oudescens Schodde, yar. nov.

Affinig varietatis fenuifoliae, sed habito + minore, maturitate praccociore

forum eypselarumque, corollis + dellexis, et pappo reducto differt.

Tyres: RB. Schodde 9144: AD95908093 (holatypus ): South-west Murray Mullve,

East side of the Chauncey’s Line-Monarto South road, ca. 3-1 km north

of the junction ot Chauneey’s Line and the Chauncey’s Line-Monarto South

road, which is ca, 19 km south-west of Murray Bridge, Growing on grey

sand. Corollas lemon. 4.X%.1958.

Erect virescent to grey herb, differing from var. fenuifolia in ity frequently

smaller size, being (%)15-6(6%) om tall with 1-10(+ 40) flower heals. the

relatively earlier maturation (by several days to ahout a week) of its Horets

and eypselae, its + deflexed corollas, and its reduced pappus which yaries from

a ring of 20-30(40) dentate setae of unequal length + 4 length of corolla to

+5 unequal setae in number, or tu a ring of minute scales in size (Fig. 3).

The reduced pappus is the principal distinguishing character of this variety,

Seecmirens ExXaAnunep

Sour Ausiparia: — Anonym, (Herb, J. M. Black); AD95731023: Karoonda. 5.X.1'915,

pu. — £. WW. Ising #n.; AD95909057; Ca, 2 ko west of Murray. Bridge. 9X. 1948. —

il. Sehoidde 493: AD95807142: Field Naturalists’ Sogiety Sanctuary at Chameey’s pin

I4.1%.1957, pp. — RB. Schodde 849: ADSAGNSI74: Channcey’s Line, ca. 0-6 kin east of the

junetion of Chiuncey’s Line aud the Chauncey’s Line-Monarto South road. 6.1X.1958. pp.

— R. Schudde 9i4a: ADIS9O8NG3; Ca. 3-1 kin north of the junction of Chauncey’s Linc and

the Chauncey’s Line-Mouarto South road. 4.X,1958, (type). — P. G, Wilsonw 2029: AD

96203135; Ca. 50 km north of Bordertown, near Bunn's Bore. 27.VIIL1961. pp. — P. G.

Wilsan 2124: AD96201145: Ca. 97 km north of Bordertown on Pinnaroo-Rordertnwn reac.

AO.VITLI961. p.p.

is s

bee is

& q fi

eS my

E 4 ba

8 i: ae

4 ‘A

Fig. 8. Millotia tenuifelia var. nudescens Schodde. A, whole plant (type—Schodde

14a); B, mature flower head (type—Schodde 9149); C, mature florets showing variation in

pappus (type—Schodde 914a); D, whole style and androceium (type—Schodde 14a).

936 R, SCHODDE

Disvarawiion, Ecotocy axnp Moreuorocicar Variation

South Murray Mallee and upper 90-mile Desert of South Australia, probably

extending into the Big Desert of Victoria. Throughout its range, it grows side

by side with var, tenuifolia.

In the Chauncey’s Line area, M, fenuifolia in its fully pappose form is

found vommonly thronghout. beth on the whitish sand ridges and intervening

red sandy flats; the reduced pappus form is restricted to the whitish sand ridges.

slightly predominating there in numbers over fully pappose plants, The degree

of reduction of pappus is the same for all florets in any one plant. Or the

sand ridges, plants with fully developed pappus, plants with completely reduced

pappus, and plants showing various degrees of pappns reduction grow side hy

side. The reduced pappus forms tend to flower und mature seed earlier than

fully puppose forms and this may haye survival advantage because the sand

ridges are probably prone to earlier spring dessication than the surrounding

low-lying Idamy Hats,

MoxpesovoucaL Variation ix Millotia tenuifolia

A strikingly uniform species throughout its range, the only distinct variant

being the form with reduced pappns in the lower Murray Mallee of South

Australia. Tasmanian plants often have slightly larger Hower heads and in-

volueral parts than those on the Australian mainland,

The type collection of Millotia hispidula Gdgr. is a mixture of specimens

ot M. tenuifolia and M. myosoficdifolia. Jt appears likely that Gandoger did not

cheek the types of these latter names nor Steetz’s enumeration (1845), confused

M. myosotidifolia with M, tenuifolia, and hence described the specimens with

pilose (or hispid) hairs as a new species. A lectotype has been chosen,

ARVINITIES BETWEEN THE SPECIES OF \Lillotia

M. myosotidifolia is not closely allied to anv other species of Miflotia. The

shape of its leaves, involucral bracts, und evpselace with their elongate appressed

papillae, and its pappus of toothed setae which usnally tend to subplumose at

the apices render it obviously distinct.

In its assemblage of morphological characters, MJ. greevesii is somewhat

intermediate between M. myosotidifolia on the one hand, and M. maerocerped

and M, tenuifolia on the other, yet is not closely related to any. It resembles

M, imyosoticlifolia in its floral merphology and the other two species in its leaves.

indumentum, cypselue, and cypsela papillae.

M. macrocarpa and M, tenyifolia are closely allied, tle fundamental simi-

larities Iving in the floral parts and cypsela papillac. The distribution of the

two species overlaps at least in the Gawler Range region of South Australia,

though both oceur in different ecological sites and M. macrecarpu towers

earlier.

That M. tenuifulia and M. myosotidifolia were not distinguished since 1853.

despite their many differences, is due to the fact that the species of Millotia have

been hitherto recognised hy the character of the pappus rather than that of the

floret and cypsela. Both species occur close to each other over much of their

Vie. 9, Intermediate fonn between Millotiz myosuttltfolia (Benth) Steetz and M. tenui-

folia Gass., lew. Teal: MEL. A, involneral bract; B, whole floret; C, whole stvle and

androecium,

Type of Millotia depauperata Stapf. D, showing floret, style, anc androecium, though

the form of the eypsel papillae may not be avcurate. (By courtesy of BR. Melville,)

238 R. SCHODDE

range. Where this happens, at least in southern South Australia, they are usually

separated by their preferences for diffcrent soils, M. myosotidifolia being found

on loamy sands and M. tenuifolia on less fertile sands and sandy clays, and

different flowering times, that of Mf. tenwifolia being up to several weeks in

advance. There is, however, among a mixture of M. myosotidifolia and M.

tenuifolia in MEL collected by Heal at the sources of the Swan River in 1889,

a single specimen which combines the character of one or other of these species

and perhaps indicates that hybridisation may sometimes occur (Fig. 9, A-C).

a Thy ] |

\ \ i |

| " ‘ \ ! 4 /

Mare 4 ; ' F j

aes Se See ol j ji.

we t \ \ \ . | :

: j on ary j —

i } ¥ ae

N ‘

\ ate TG _ —_

Fig, 10. Map 1—Disiribution of Millotia myosotidifolia (Benth.) Steetz.

Map 2~—Distribution of Millotia greevesti F. v. Muell. var. greevesii @, var. glandulosa

Schadde *; var. kempei (F. v. Muell.) Schodde +: var. hebnsii (F. v. Muell. and Tate }

to glandular-haired involucres in var. helmsii. Line 2 indicates region of change of woolly

to glandnlar-haired invelucres in var, glandulasa.

TAXONOMIC REVISION, GENUS MILLOTIA CASSINI

4 + |

/ i wed

/ |

dus d

! H

ie !

ie ‘ j

} Sl |

| (i Ssag

{

| i

“IY = cy ]

' .

( A

a ‘

\ you

\ ue

\ \ —

; kK 1

\ He y | ’ :

\ h a ee mt ;

\ * i

\ aa | f /

\ ( j

\ oa. ;

\ 4 wee 1 we

\ \ \ “

\ \ \ !

‘m \ \ \ H +

\ \ ; re

\ \ '

Bae te \ \ |

: \ \ | [

i \ es.

Vig. 11. Map 3—Distribution of Millotia macrecarpu Schodde.

Mup 4—Distribution of Miflotia tenuifolia Cass, var. tenuifolia 3; var. nudescens

Schodde @.

ACKNOWLEDGMENTS

I wish to thank the Curators of all herbaria who made available loans or

donations of material, those members of the staff of the Kew herbarium and

particularly Dr. R. Melville for submitting details of their collections of Millotia,

Dr. N. T. Burbidge for photographs of several types, Mr. R. T. M. Pescott for

allowing me to examine type specimens held in the National Herbarium of

Victoria, Dr. Hj. Eichler and Messrs. E. N. S, Jackson, D. N. Kraehenbuehl,

D, J, E. Whibley and P. G. Wilson for their efforts in field collecting, the Adelaide

240 R. SCHODDE

University Zoology Dept. and Adelaide Botanie Garden for making available

facilities for germinating and growing seeds, and Miss C. M. Eardley and Mr.

P. G. Wilson for their advice and eriticism.

Tam especially grateful to Dr. Hj. Kichler for making available the facilities

of the State Herbarium of South Australia and his invalmable encouragement,

criticism, and assistance in the execution of this study.

REFERENCES

Battex, F. M., 1900. The Queensland Flora, 3, p. $43,

Bentnans, G., 1867. Flora Australiensis, 3, p. 595,

BentoHam, G,, 1873. In Bentham & Hooker £., Genera Plantarum, 2, p. 313.

Buentuam, G., 1873a. Notes on the Classification, History, ancl Geographical Distribution

of the Compositae. Journ, Linn. Soc, (Lond,), 13, p. 424.

Buacx, J. M., 1919. Additions to the Plora of South Australia. No. 15, Trans. Roy. Soe.

S. Austral, 43, p. 43.

Biacr, J. M., 1929, Flora of South Australia, 4, p. 638.

Brace, J. M., 1957. Ihid., ed. 3, 4, p. 916.

Bunuigr, N. T., 1960, The Phytogeography of the Australian Region, Austral. Journ. Bot.,

8, p. 79,

Cassini, H., 1929. Tableau Synoptique des Synanthérées. Ann. Sci. Nat., 17, p. 416.

Davis, G, L. 1952, Revision of the genus Calotis R. Br. Proce, Linn. boc, N.S.W,, 77,

p, 161.

Dr Cannonie, A. P., 1638. Procdromus Systematis naturalis regni vegetabilis, 6, pp. £61, 371.

Droucr, G. C., 1917. Rep. Bot. Soc, and Exch. Clib Brit. Isles, 4, p. 646.

Ewart, A. J., 1931, Flora of Victoria, 1139,

Gasuocrr, M., 1918. Sertum plantarym navarwn, 1, Bull. Soc, Bot, France, 65, p, 45.

Horraany, K., 1690. Tn Engler and Prantl, Die Nattrlichen Planzenfamilien, 4, 5, p. 191.

Hooker, J. D., 1856. Flora Tasmaniae, I. p. 209.

Lesree, A., 1943. Dictionnaire Descriptif et Synonymique des Genres de Plantes phanéro-

games, 8b, p, S85,

Lessing, C, I., 1832. Synopsis generum Compositarum, p. 273.

Mvexurn, F. von, 1662, Fragnuenta Phytographiac Austruliac, 3, p. 18.

Mveuien, F. von, 1882. Australian Plants (mew or imperfectly known). The Southern

Science Record, 2, p, 2,

Muysven, F. von, and Tarr, R., 1896. ScientiGie Results of the Elder Exploring Expedition.

Botany. Trans. Roy. Sec. S, Austral, 16, p. 368,

Srapr, O., 1910. Kew Bull, 1910, p, 22,

Steer, J. 1845. In C, Lehinann, Plantae Preissianae, 1, pp, 456-458.

TAXONOMIC REVISION, GENUS MILLOTIA CASSINI

Ixpex To Names (alphabetical)

Italics indicate synonyms; numbers refer fo pages

Calotis squamigera C. ‘I, White

Chevreulia Cass.

Conyza Less.

Erechtites Rafin.

Eurybiopsis DC.

Ixiolaena Benth.

Leptorhynchos Less,

Millotia Cass,

depauperata Stapf

glabra Steetz

greevesii F. v, Muell,

subsp. greevesii

var. glandulosa Schodde

var. greevesii

subsp. kempei (F. v. Muell.) Schodde

var. helmsii (F. v. Muell. & ‘late) Schodde

var, kempei

hispidula Gdgr,

kempei F. v. Muell.

macrocarpa Schodde

myosotidifolia (Benth.) Steetz

var. glabrescens Sond,

var. robusta (Steetz) Sond.

robusta Steetz

tenuifolia Cass.

var, nudcscens Schadde

var. tenuifolia

Quinctia Cass.

urvillei Cass.

Seyphocoronis A, Gray

majus (Turcz.) Druce

Senecio (Tourn.) L.

myosotidifolius Benth.

Toxanthes Turez.

muelleri (Sond.) Benth.

Toxanthus Black (= 'Toxanthes)

whitei Black

Waitzia Wendl,

241

TWO NEW ECHIUROIDS (ECHIUROIDEA) FROM AUSTRALIA

BY S. J. EDMONDS

Summary

Two new echiuroids are described from Australia, Listriolobus bulbocaudatus from Moreton Bay,

Queensland, and Ochetostoma myersae from Long Reef, New South Wales. A key to the genera of

Australian echiuroids is also given.

TWO NEW ECHIUROIDS (Echiuroidea) FROM AUSTRALIA

hy S.. J. Eomonps*®

[Read 13 June 1963]

SUMMARY

‘Two new echiuroids are described from Australia, Listriolobus bilho-

cdudatuy Frou Moreton Bay, Queensland. anc Ochetostuma myersae fram

Long Reef, New South Wales. A key ta the genera of Australian echinroids

is also given.

Listriolobus bulbocaudatus n. sp.

(Plate 1, Fig. 1)

Listrinlohus Fischer, 1926, p, 110; Fisher, 1946, p. 233,

Material: Four specimens dredged from 8-10 fathoms, west of Mud Island.

Moreton Bay (Queensland): coll. Prof. W, Stephenson (University of Queeus-

land), Ang., 1962.

Description: The specimens are sausage-shaped. The length of the trunk js

48-80 mm. and the maximum width is 14-20 mm, The probescis (still attached

to the body in all specimens) is, in the preserved condition, short, stout and

rounded, about 10-16 mm. long and about as wide. The trunk is dark reddish-

brown but the proboscis is much lighter in colour. A feature of all the specimens

is that the posterior extremity of the trunk is expanded into a fleshy, bulbous

structure, light pink in colour like the proboscis. The bulb is slightly pointed

posteriorly and bears a sumber of rings af very large, prominent, wart-like

papillae. The trunk is covered with whitish papillae that are easily discernible

to the naked eye. They are closely packed posteriorly and anteriorly and Jargest

posteriorly.

In three of the specimens the Jongitudinal muscles are grouped mto seven

bundles that are best seen on dissection, The body wall of the other specimen,

the smallest, is very thin and the muscle bands are not as well-defined. The

oblique musculature between the longitudinal bands is not grouped into fascicles

as it is in the genus Ochetostoma. There are two relatively long setae connected

internally by a well-developed interbasal rvuscle. There is a well-developed

mesentery attached to the anterior part of the oesophagus and the body wall.

The alimentary canal is very long and much coiled and contains sausage-

shaped faecal pellets. The walls of the pharynx, oesophagus, gizzard and crop

are thicker than those of the intestine, The siphon is not very prominent. There

is a caccum near the posterior extremity of the alimentary canal and a ventral,

ciliate groove which terminates at the caecum.

Trans, Roy, Soc, S. Aust, (1963), Vol. 87.

o44 5, J. EDMONDS

sitle wad two on the right side (dorsal view), No trace of a third on the right

side avas discernible, The presence of this extra nephridium is diffienlt ta

explain. Fisher (1946, p, 222) reported the presence of three nephridia on one

side and two on the other in a species of Lissomyema (Thalussema) smellita

Conu, L. meéllita is regarded as possessing two pairs of nephridia, In the

Queensland specimen the region of the nephridia near the body wall is globular

in shape, the rest tubular. ‘lhe nephrostomal lips of all the nephridin are verv

long and mach coiled, mmch more so than those of L, hexamyorus Fisher (1949,

plate 29) and L. pelodes Fisher (1946, plate 22),

The blood systern cesenbles that of L, pelodes. The intestinal vessel makes

contact with the crop where it oxpands into a thin-walled structure of lure

diameter. There iy a ring vessel which gives off two neuro-intestinal vessels

that join before they reach the interbasal muscle and then, in two specimens at

least. bifureate to form a Toop around the musele, The ventral vessel suns close

ta the nerve cord and terminates at the rectal caecum.

The anal vesicles are Jong, thin and brown in colour, They are nat swollen

near the rectum. They bear mumerous synall ciliate funnels with short stalks

Systematic Position: These specimens fall into the genus Listriolofus

(Fisher, 1949. p. 480). "They differ from L. hexamyotus Fisher (1949) whieh

has six longitudinal muscles and one pair of nephridia, feom L. bahamensis

(Fischer, 1926) which has 16 lemgitudinal muscles, from F., pelodes (Fisher,

1946) which has eight bands, froma 1, rikivensis Sato, 1939, whieh has twelve

bands. and from L. sorbillans (Lampert, 1883), already reported from Sydney

by Augener (1903, p, 349), which has thirteen rouseles. A near species is

Thalassema formulosum Lampert, 1883, which Fisher (1946) placed in the

genus Ochetostome. Tt has 7-8 nusele bands, two pairs of nephridia with

spirally-eoiled nephrostomal lips und sparsely distributed white papillae, Fisher,

however, must have had evidence that the oblique musculature between the

muscle bands was grouped into small bundles, Neither Lampert (1883) nor

Whurton (1973) mention the posterior swelling of the trunk in their description

of I. formulosum, Thalassema exilii ¥. Muller has 8-10 muscles and two pairs

of nephridia. Lts nephrostomal lips ave folded and crinkled but not elongated,

Fisher (1946, p. 24) thinks that it is probably a Lissomyeme.

Through the kindness of the authorities of the U.S. National Museum,

Washingtun. T have been able to compare these specimens with) a dissected

specimen of L. pelodes. The latter, US.N.M. Cat, No. 20622, was collected

wt Tomales Bay and identified by Fisher. Most of its internal strictures: were

damaged. The specimen, however, lacks the bulb and posterior rings of

papillae that are found on all the Australian animals and its proboscis is long

and thin.

Jonsequently it seems reasonable to regard these specimens trom Queens-

Jand, although close to L. pelodes, O, formulosum and T. exilii, as new. It is

of interest to note that L. bulbocaucatus was dredged from a mud bank very

much is L. pelodes was by Barnard and Hartman (1959) in California.

Diagnosis; Body sausage-shaped und probosvis short and stout. In older

specimens the longitudinal musculature is grouped into seven bundles; in

younger specimens this is not sa apparent. Oblique musculature between the

laneitudinal mnsecles not grouped inte small tingslles, Two pairs of nephridia

arise behind the setue. In the bwo largest specimens there are three nephridia

on one side and two on the other. A stout fastening mesentery is connected

TWO NEW ECHIURGIDS ( ECHIUROIDEA) FROM AUSTRALIA 245

t6 the oesophagus, Posterior region of the truuk is swollen inte a Jight-pink,

fleshy, bull-like structure, Body covered with whitish papillae which are warty

and arranged in a number of rinys on the posterior swelling.

fype Specimen: Australian Muscum, Sydney,

Type Lovality: Mud Tsland i Moreton Bay, Queensland,

Ochetostoma myersae jsp.

(Plate 1, Fig. 2)

Uclivtastonia Tawekurt and Tiippell, 1828; Fisher, 19445. p. 240,

Speclimens; Four (three dissected), Aust. Museum collection W 3757,

Locality: Long Reef, near Sydney, New South Wales. Collected by Miss

D. Myers, 20-4-62.

Deseription; The specimens are sac- or sausage-shaped. The anterior region

Mm the tronk tends to be rounded while the posterior region is more pointed,

The animals were described by the collector as being “chlorophyll green” in

colour, Preserved tn alcabol they are pink, The length of the trunk in 20-35

mm. and the maximum width 9-15 mm. The surface of the trunk is covered

with soft, white, wart-like papillae which are largest and most noticeable in the

posterior third. The proboscis, which was still attached in three specimens, is

about ¢ quarter to half the length of the trunk, It tapers slightly antetiarly and

in the fixed specimen is almost tubular in shape.

The longitudinal muscles are grouped into 18-21 bundles that are usually

visible externally but which are best counted in dissected specimens. In two

specimens two muscles anastomose, The longitudinal muscles lie close together

and are most strongly developed over the anterior half or two-thirds of the

trunk, The oblique muscles between the longitudinal hands are grouped rather

weakly into fascicles aud not into such strongly develuped bundles as they are

lie posterior to the setae, The nephrostomes are expanded inta two elongate,

thread-like lips which are rather weakly coiled. In the largest specimen only

one pair of nephridia could be found.” The nephridia of this specimen were

larger than those of the other two dissected specimens and not as coiled as those

shown for QO, edax Fisher (1946) p. 14). This variation in the aumber of

nephridia is puzzling, “There seems nu doubt, however, that since all the speci-

mens look alike and were collocted at the same time and in the same locality

they belong to the same species. There are two prominent setac and a stron

interbasal muscle. Three or four strong and prominent muscles connect each

seta and the body wall. The alimentary system consists of {1) 9 comparatively

short foregut which extends as far ag the ving vessel of the vaseular systern, (2)

a thicker intestine with a ciliate groove and a collateral intestine, and (3) & short

rectum which bears a small caecum. The contents of the canal are very coarse

and not formed inte pellets. The vascular system consists of a dorsal vessel, <

ring vessel, two neuro-intestinal vesscls anda ventral vessel, The neuro-intestinal

vessels join und then split again to enclose the interbasal muscle, The anal

vessels are long and thin and do not branch. The ciliate funnels ure borne on

very short stalks,

Systematic: Position: These specimens closely resemble O. haronii (Greef,

INTY) and O. eax Fisher, 1946. QO. buronit possesses 17-19 longitudinal anusele

bands und O. edax 16 or 17. Short branching outgrowths ure present on the

446 §. |. EDMONDS

anal vesicles of O, baronii. Such structures are not present in the specimens

from Long Reef. Fisher (1946) says that the normal number of muscle bands

of Q. edax is probably 16. Through the kindness of the authorities of the U.S,

Natioual Museum, Washington, I have been able te compare the Australian

specimens with a specimen of O. edax from Puerto Refugio (U.S.N.M. Cat. No.

20623). It was identified by Fisher. It is a small specimen with a deciduate

probuscis, It possesses fewer longitudinal muscles than the Australian speci-

mens, its body wull is much thinner and the papillae are more preminent,

especiully in the mid-region of the trunk. Consequently the specimens trom

differs from O, australiense Rdmonds, 1960, in the number of its Jongitndinal

muscles and in the rmimber and position of its nephridia,

Diagnosis; Trunk sac- or sausage-shaped, posterior region somewhat pointed.

Trunk bears numerons white, wart-like papillae which are most noticeable on

the surface of the posterior third. Proboscis not readily deciduate, about

quarter te half the length of the trunk and tupering slightly anteriorly. 18-21

longitudinal bundles. placed closely together. Oblique muscles between the

hundles weakly developed. Two pairs of nephridia which lie posterior to the

setae (une specimen has only one pair of nephridia), Nephrostomal lips

elongate and weakly coiled. “Two prominent setae and a strong interbasal

muscle, Rectal caecum, Contents of alimeutary canal very coarse and nel

formed into pellets, Vascular system as in O. australiense and O. edax. Anal

vesicles long, thin and unbranching, Ciliate funuels ou very short stalks. When

alive chlorophyll green in culour.

type Specimen: Australian Muscum, Sydney.

Type Locality: Long Reef, new Sydney, New South Wales.

KEY TO THE GENERA OF AUSTRALIAN FCHIUROIDS

This key replaces the one gicen in Edmonds, 1960

1, Proboscis usually conspicuous (although sometimes deciduous if speci-

mei is handled) and often several times the length of the body but never

bifid. Anal vesicles long, sac-like. unbranched and covered with minute

ciliate Furmels —family Echiwidae _, ri ers. 2

Females with elongate, bifid proboscis. Anal yesicles with many branches

that end in ciliate cups. Male degenerate, living in or on the fermale —

family Bonellidue ~ lf. io as fo ee aw Dis I

3%. Longitudinal muscles of hody-wall grouped into bundles —_ 5, 6

4, Longitudinal muscles of body-wall nut grouped into bundles =. 7, 8

5, The interval between the bundles is crossed by numerous separate, smull

bundles: of the inner oblique layer. Nephridia with spirally coiled,

nephrostomal lips — genus Ochetostomea.

6 Tle interval between the bundles is not crossed hy matnerous separate,

small bundles of inner oblique layer; nephrostomal lips elongate and

spirally coiled — genus Listriolobus.

Nephrostomal lips either coiled or expanded into leaflike structures 9, 10

% Nephrostomal lips neither coiled nor expanded into leaf-like structures: —

venus Thalassema.

9, Nephrostomal lips long and spirally coiled — genus Anelassorhynclius,

TWO NEW ECHIUROIDS (ECHIUROIDEA) FROM AUSTRALIA 247

10, Single pair of nephridia with nephrostomal lips produced to form leaf-like

structures. Proboseis long, deciduous and slender with a small fan-like

extremity — genus Arhynechile.

Ui. Only one nephridium or uterus present. Coelomic aperture of the nephri-

dium is situated near the base of nephridium at the end of a short

lateral tube — genus Bonellia.

12. More than one nephridium or uterus wee: ; ; ww. 13, 14

13. Two nephridia or uteri with nephrostomes placed near their distal ends.

Male permanently lodged in a small blind tube which opens between the

nephridiopores — genus Pseudobonellia.

14. Third nephridium placed between two paired nephridia — genus Archi-

bonellia,

REFERENCES

Aucener, 1., 1903. Beitrige zur Kenntnis der Gephyreen nach Untersuchung der im Got-

tinger zooligischen Museum befindlichen Sipunculiden und Echiurden. Arch. f.

Naturgesch. (1), 3, pp. 207-370.

Barwarn, J. C., and Hantaan, O., 1959. The sea bottom off Santa Barbara, California.

Biomass and Community structure, Pacific Naturalist, (1), 6, pp. 1-15.

Epsronns, S. f., 1960. Some Australian echiuroids (Eehiuroidea). Trans. Roy. Soc. 8, Aust,

83, pp. 89-98.

Fiscuer, W., 1926. Sipunculiden und Echiuriden der Hamburger Siidsee-Expedition 1908-

1909, Mitt. zool. Staatsinst und zool. Mus, Hamb., 42, pp. 109-117.

Fysnen, W. K., 1946. Echiuroid worms of the north Pacific Ocean. Proc. U.S, Nat. Mus,,

96, pp. 215-292.

Fisuern, W. K., 1949, Additions to the echiuroid fauna of the north Pacific Ocean. Proc,

U.S. Nat. Mus., 99, np. 479-497,

Lamrerrr, K,, 1883. Wher einige neuc Thalasserna. Zcitschr. wiss Zool, 89, pp. 334-342,

Sato, H., 1939. Studies on the Echiuroidex, Sipunculoidea and Priapuloidea of Japan. Sci.

Rep. Tohoku Imp. Univ. Ser., 4 (14), pp. 339-460.

Wrarron, L. D., 1913, A description of some Philippine Thalassema with a revision of the

genus. Phil. Journ, Set. Ser. D (8), pp, 243-270.

EDMONDS

1. Listriolobus bulbocauclatus

(1-5 x natural size).

s. Roy. Soe. S.A.", Val, 87

Ochetosloma

(28 natural size).

PLATE

NUePSUe

OBITUARIES: HERBERT WOMERSLEY

Summary

OBITUARY 245)

HERBERT WOMERSLEY.

ALS. (Hox, Causa}, FAVES,

1889-1962

Herbert Womersley died in Adelaide on the 14th October, 1962. Althuuch

he was aged 73 years, and was subject to increasing ill-health, he had worked

on the classification of the Acarina until within a fortnight of his death, Although

without formal University training, he was a world authority upon the Acarina,

and, at an earlier period, the Apterygota. We was able to accomplish a great

deal in descriptive taxonomy, in which in fact he had few equals, owing to his

intellectual discipline und methodical habits of work. His contribution to the

subject of acarology will be considered in another memoir, and separate treat-

ment will also be given to his career as an entomologist, both in the economic

und taxonomic spheres.

Womersley was born at Warrington, Lancashire, England, on 10th April,

1889, He trained as an industrial chemist, and it was not nntil 1930 that he

was uble to transfer into the professional ranks of entomolovy. His interest tn

biology was life-long, and commenced with « youthful interest in entomology.

no doubt fostered by his father, who was an enthusiastic amateur lepidopterist.

Womersley’s early interests in entomology were the Lepidoptera and the Diptera.

While stlla yvonth he was attracted by microscopy and microscopical technirjue,

and had the good fortune to be mstructed by Abraham Flatters in Manchester.

Ont al this came his first publication, on the use of terpineol as a clearing agent

(1912). ITe served in the Imperial army in 1914-1917, firstly in the Royal Army

Medical Corps, through his St. John Ambulance Brigade training, and then im

the Chemical Corps of the Royal Engineers, serving on the Western Front. In

IQIT the denyund for trained chemists was intense. We was recalled to Eng:

land and discharged to explosives manufacture, both there arid in Scotland,

until the war was over, by 1920 he left Warrington for Bristol, and while em-

ployed there he was able to resume his entomological studies.

im addition to these effurts. he took a prominent part in natural history

societies in the west of England. He served a term as President, Bristol

Naturalists Society, and was also one of the promoters of the South-Western

Union of Naturalists, acting as Secretary from its Inception until he left England.

He worked to such purpose that within a few years he was the leading British

authority on the Apterygota, particularly the Collembola and Protura. eaten

callections were referred to him for working up as well us material from the

British Isles. Ih 1930 he was appointed Entomologist, Section of Pasture and

Field Pests, Division of Eeonomic Entomology, C.S. & LR. (now C.S1.R,0).),

lis work had attracted the attention of R, J. Tillyard, the author of the well-

known text book, “Inscets of Australia and New Zealand”, and who later became

the Chief of the Division,

After induction and training periods at the British Museum and in Sonth

Africa, Womersley took up his duties in Western Australia. Here he was given

the dificult assignment of developing or improving methods of control af the

two major pasture pests, the “lucerne Hea”, Sminthurns viridis (L.), and the

Redtegged arth Mite. Hulotydens destructor (Tucker). In this field his new

contibution was the sthidy of possible control of Sminthurus by predatory

bdellid mites. The results achieved were considered promising, thowich ham-

0 OBITUARY

pered by the financial stringeuey then ruling in Australia, and reluctantly he

resigned his position ta take up the appointment of Entomologist, South Aus-

iralian Museum, in 1983. The study of the effects of these predators wus

continued by other workers in the Division, with Womersley ucting as a

ermsullant in the taxonomy of the Collembola and the Acarina, A more

detailed story of this work will be tald in another study.

At the South Australian Museum Womersley was able to devote much of

his time to continuing his studies on the taxoueny of the Apterygota. Ile was

uble to produce a large amount of work, incliding publishing a large paper

on this group in the Transactions of the Royal Society of South Australia in

1933, as well as two short papers on the Acarina in the same year. These two

major taxonomic fields were pursued with great Vigour, His studies on the

Australian Apterygota culminated in 1939 in the “Primitive Insects of South

Australia’, which jn actual fact monographed the whole of the Australian Eunna

then known, Possibly attracted more by the larger unworked arca ol the

4earina, he devoted increasing attention to this group. The material from the

Berleso funnels was now examined mainly for Acurina, and) simultaneously

collections: of free-living and parusitie mites were studied. Ineressingly re-

quests for identifications came to Womersley, and he finally was prepared to

identify mites in nearly overy category snbmitted, This was no smull order,

since ultimately the Acatina may begin to rival the insects in the number of

species and higher aitegories, Again. a separate memoir will be uccessary lo

wive in any detail the extent of Womersley’s studies in this group. Els unajor

work was his monograph of the trombicnlid mites of the Oriental and Australasian

regions, published in 1952. In this the immense collections that had been re-

ferred ty him from field workers, particularly teams studying, the epidemiology

of scrub typhus over the “Austra-Asian area”, were brought into systematic order.

This work remains the most complete weeount of the wombiculid mite faunu

of this region, even though, in the ten years since it has been published, many

of the taxonomic categories have since Ween changed. with the intense continu

ing studies of these mites. Among workers responsible may be mentioned R.

Domow of Queensland, who received initial training from Worersley in

Adelaide.

In 1954 Womersley retired as Entomologist, South Australian Museum, but

was immediately re-appointed Acarologist, a salaried position created specially

for him. Tle retired from this in 1959, at the ave of 70, but immediately again

became Tlonorary Acarologist, and continued his systematic habits of work,

Following the production of his 1852 monograph, he was able to produce a

large number of shorter papers on the ‘Trombiculidae and many other families.

Increasingly he devoted his efforts io the Mesostigmata, which had leen com-

paratively neglected,

Inmnediately on coming to South Australia in 1933 he took the interests

of the Royal Society of South Australia to heart, serving im succession in every

office on the Council aver a number of years. These were ne sinecures, as they

included the task of Editor for the six years 1937-1943, and Treasurer Cur Four

veurs (1950-1, 1956-9). He served as President in 1948-4, and [rom 1945 on-

wards he was the Societys representative an the Flora and Iguna Protection

Canmittee which was advisory to the Minister of Fisheries and Game, Com-

mencing with his period as President, he was later (1945) appointed a Com-

tissioner of The National Park in his own name (later the Commissioners of

The National Park and Wild Life Reserves with their expanded scope}. He

identified himself closely with wildlife preservation in the State, ane his duties

OBITUARY 31

as a Commissioner gave him a great deal of pleasure, At one mocting, which

the writer had the honour to aftend, it was amounced that Womersley had

allended 68 meetings without any absence. This was a remarkable record,

particularly in view uf the ill-health which he suffered. He continned to attend

until the record stood at 91 meetings over eight years. It was fitting that at his

funeral the Rangers of the National Parks in their grey-green uniforms Formed

w vuard of honour.

Jn 1943 he was awarded the Vereo Medal of our Society. In 1962 another

hanow was bestowed, in his being elected Monorary Fellow, a fitting tribute

to his scientific achievements and his long service to the Society, Angther

hhovour which he greatly valued was his election as Associate of the Linnean

Society (Honoris causa), in 1929, He was also a member of the Linnewn Society

of New South Wales (1934), and a Fellow of the Royal Entomological Society

(1926). On Jeaving Bristol for Australia in 1930, the Bristol Naturalists’ Society

so bestowed upon him the tide of Honorary Member, as a mark of appreciation.

Most of his time, over the last 30 yours of his life, was spent in South

Australia, and as the years progressed his wn collecting fell to quite small

proportions, exeept on special trips. Thus he travelled to New Guinea in 1954,

re also (1952) made a trip to New Zealand, His major travelling in his final

deeades was a visit to North America and Europe to study acarology, under a

grant [ov this purpose (the study of the vector mites of scrub typhus and serub-

itch, the Trombiculidae) from the United States Public Health Department,

Tle was gratified to be able to meet personally his colleagues in these somewhat

restricted groups, as well as a number of the more general students of the

Acarina, particularly the continental students of the acari diverst.

Womersley was twice married, By his first wife he had twa suns, J. §,

Womersley and H. B, §, Womersley, both botanists, and both members of this

Soniety.

lie lias lett behind him the legacies of a vast amount of publication in

descriptive taxouemy, more particularly so in the Acarina, and the reference

collection of the Acarina in the South Australian Museum is one of the vreat

collections of these arthropods. for the world.

The reference list of Womersley’s publications will be given elsewhere,

ane more detailed accounts of his taxononiic work. His colleagues had a warm

appreciation of his gifts and industry, Lis name is commemorated in a nuniber

of tava in the Arthropoda, aud these are given helow.

Genera named for Womersley

ACARINA,

Wermersia Wharton, 1947. J, Parasitol 33 (4): 381. Type species W. atrandtmad Cate Tor

stranimanni), Wharton, Joo. cit. (Vrombiculidae t.

Womersteyessta Meteor, 1953. Fanta Re P. Rom. 5 (1): 15%,

Type species not desiematerdl ( Trambidiidae }.

Wormersleyia Radford, 1946. Parasitol, 37 (1-2), 48,

Type species W.. mingta Radford, U94G6, for, cit, p. 51.

Womersleygua Vervommen-Grandjean, 1960, Acarologia, 2 (4)) unpaged table between pages

1) aml 47. Type species Troverdhula geckubiq Wamersley, (952 (‘Lrormnbiculiday),

COLLEMBOTA

Wonerleya Denis, 1948. Notes But. chin, Slumuhai, $2; 198. Sype species Protumnura

hieina Dents.

Womersteyalfa Sultaub, 1944, Ree. Dominion Vii NZ, bs 142. Type species Womersteyelle

mieeata Sulmon, Joe. cit. {lsotomicue),

Womendenmeria Stueh, 1949. Aeta monogr. Cracow. yy. Gb Annridue, Types spocies Cerus

trimeria hicornis, Wamersley, (940,

252, OBITUARY

Specicy named for Womersley

CRUSTACEA

Quasimedin ricomersleyi Sheard, 1936. Bec, 5. Aust. Mus, 3 (4): 464 (Amphipoda,

Phliantidag ) .

ACARINA

Agaue parva womersteyi Viet, 1950, Wurther zool, Results Swed. Antare. Exped. 1904-L903,

4,3: 44 (Halacaridue),

Austromhicula, womersleyi Laverence, 1949. Ann. Nat. Mus., 11 (3): 419. for Leeuwen-

hoeki« womersleyi Lawrence, 1948, Parasitul, 39 (1-2): 41 (Trombiculidac).

Cullidosoma avomersteyi Sonthcott, 1946, Proc, Linn. Soc. N.S, Wales, 7h (1-2): 43

( Birythraeidge).

Ceratocclaenopsis womersleyi Veigirdh, 195(), Ark, f. Zool, (2) 1 (24): 384 (Celaenopsidae),

Cunaxa womersieyt Buker and Hollman, 1948, Anales, Escuela Nae. Ci. Biol. Mexico, 5

(3-4); 234 (Cunasidae).

Erythraeux wemersleyt Southeott, 1946. Proc. Linn. Sac. N.S. Wales, 71 (1-2): 40

(Frythtaeidae).

Purdie jopmersteut Vercammen-Grandjean, 1933. Rey. Zool, Bot. ufr., 48 (1-2): 19 (Trom-

niculidac ).

Uoleothrombidium (sic, for Holectrombidium] woumersleyti André, 1948. Bull. Mus. Nut.

Hist, Nat. (3 20 (2); 159 ( Trombidiidac).

Hytioispis penne eyt Domrow, L957. Prov. Linn. Soc, N.S. Wales, 81 (3): 205 (Phyto-

sedidac).

Leeuiwenhockia womersleyi Lawrence, 1948. Parasitology, 39 (1-2): 41 (subsequently type

species of Austrombieula Lawrence, 1949; q.v.),

Marquesania womersteyi Lawrence, 1951, Arm, Natal Mus, 12 (1); 117 (Listrophoridae),

Paralimnochares womersleyi Luudblad, 1952. Entom. Tidsk., 73. (1-2): 23 (Tydraearina ).

Neosehdryastia womersleyi Gunther, 1940. Vroc. Linn. Soc. N.S. Wales, 65 (3-4): 254

( Trombiculicae).

Speleugnuthays teumersleyi Kain, 1955, Ann. Soc. Belg, Med. Trop., 35 (@): 695 (in key

wnly); also Rey. Zool, Bot, afrie., 50 (1-2): 21 (formal description).

Sphaerotarsus womersleyi Southcott, 1946. Prov, Linn. Soc. N.S. Wales, 70 (3-4); 177

(Simartdidae ).

Tenuipalpus womersleyi Pritchard and Baker, 1958. Univ. Calif. Publ. Entom,, rd (3):

238 (Phytoptipalpidac),

Trichowtgsines wamersleyi Damrow, L958. Proc. Linn. Soc. N.S. Wales, 83 (9): 231 ( Laclap-

ictne ) .

Tydeus wemersleyi Thor, 1932, Zool, Anz., 100 (3-4): 108 (Tydeidae).

Wharlonia wamersleyt Brennan and Dalmat, L960. Ann. Ent. Sov. America, 53 (2): 185

( Trombientidae). :

PROTULA

Evsentumon womersieyi Bonet, 1942. Ciencia, Mexico, 8 (1): 16.

DIPLURA

Anisovanipa womersleyt Silvestri, 1932. Bull. Lub. Zool. Portici, 26: 75.

Japyx (Metajanyx) aomersleyi Pagés, 1952, Rec. Canterbury Mus. &: 161.

COLLEMBOLA

Entomobryga womersleyi Beonall, 1939. Ent. Mon. Mag, 75: 101 (Entomobryidae),

Protllberpin womersley) Bagnall, 1947. Ann, Mas. Nat, Ulist.. (11) 14 (114): 442 (Tull-

bergiidae ).

Sminthurus womersleyi, Denis, 1)48, Notes Ent, chin,, Shanghai, 12; 295.

A full bibliography of Womerslev's scientific publications will be given in

the obituary notice to be published in the Records of the South Australian

Museum, where his career in entomology and his carly life will be described. A

further notice, dealing with his contribution to acarolagy, has been published in

“Acarologia” in Paris. Other short notices have also been submitted to societies

to which he belonged, or appropriate journals, The archival material from which

basic information has been obtained is in the correspondence files of the South

Australian Museum, and other material entrusted to the author by Womersley

will be deposited in the South Australian Archives.

R. V. SOUTHCOTT,

OBITUARIES: CHARLES MERVYN DELAND,

M.B., B.S., D.P.H., D.T.M.

Summary

OBITUARY pas

CHAKLES MERVYN DELAND,

M.B. S., D.POL, DTM,

1902-1962

Charles Mervyn Deland died in Adelaide on 11th July, 1962, at the com-

paratively early age of GO years. He was an authority on tropical discases

and public health, and combined these attainments with a Jove of natural history.

A revnlar attendant at meotings of the Royal Society of South Australia, he was

seledum absent tram meetings over the last decade. He served ou the Council

of the Soeicty from 1952-1960.

Deland was born in Gawler on 9th March, 1902, and was educated at

Prince: Alfred College, Adelaide. where he won many scholastic prizes, Prom

there he proceeded to the University of Adelaide, graduating M.B., 14.S. in 1924,

Jn 1926 Dr. Deland hegan his tropical work which was to continue with

few intermissions to 1950. His first appointment was as medical and quarantine

officer by the Vanikoru Timber Compuny in the British Solomon Islands after

which he joined the medical services of the Papua-New Cuineg, Territories

where he remained for nearly 20 vears. Dr. Deland’s pre-war service was ut

Kieta, Wewak and Manus with a visit to New Caledonia.

With the Japanese aggression of 1941, he enlisted in the Australian Army

aud until 1943 was stationed in South Australia where his knowledge of tropical

(liseases was useful in treating Japanese internees in Loveday camp, In May,

1943, he returned to New Guinea, serving with ANGAU, and hemg promoted tu

Teanporary Major, as DADMS, ANGAU, Southern Region, Papna, On discharge

in 1945, Le continued in New Guinea at Madang (1946-7), until completion of

his period of civilian service there, and returned to Adelaide, After shovt

locums in South Australia and a brief period of service in the Commumwvealth

Health Depuarttnent, in Darwin, he joined (1950) the State Public Health

Department, South Australia, being finally appointed Industrial Medical Officer,

During this period in South Australia he was Lecturer in Public Health to the

South Australian Nurses Board, and was Visiting Specialist in Tropical Medicine,

ivy, 1953 'Croublesome worms. No. 84, pp. 22-24,

s 1956 Mosquite theeat: possible aftermath of Murray floods. Ne. 100, p. G4,

i. 1958) Flings. No. 105, pp. 36-8,

iv, 1958 Venomous Jand animals. No, LOG, pp. 26-30.

it, 1959 Poisonous and yenemous fish. No, 110. ap. 15-22,

iv, [980 Vectors of disease in South Australia, No. 114, pp. 31-32. (A seneral

article, dealing mainly with the role of insects in public health, but

refers also ta shellfish and mammals, ) as

x 1960 Water absorbing plants, No, 116, pp. 24-87. (Refers to species of

Fuculyptes, Melaleuca and Casuarina.)

R. V, SOUTHCOTT.

OBITUARIES: HERBERT MATHEW HALE,

O.B.E. 1895-1963

Summary

254 OBITUARY

HERBERT MATHEW HALE, O.B.E.

1895-1963

Born in North Adelaide on the 3rd June, 1895, Herbert Tale spent his life

promoting biological science on two fronts — public education and research.

As Director of the South Australian Museum (1928-1960), Chairman of the

Flora and Fauna Advisory Committee (1937-1960), permanent Vice-President

of the Royal Zoological Society (since 1928), and as a member of the Commis-

sioners of the National Park und Wildlife Reserves (1936-1960), of which he

was Deputy Chairman between 1955-1960, he proved a most able administrator

and a respected advisor, and did a great deal to heighten publie interest in and

improve theic appreciation ot our irreplaceable heritage of uative Fauna aod flora.

His conscientious service to the Society led to the award of Honorary

Fellowship in 1962 following 31 years of continuous service on the Council,

during which he occupied severul senior offices, including President (1936-37 ).

Vice-President (1934-36 and 1937-38) und Treasurer (1938-50 and 1953-56).

His unselfish services to the community were recognised by his inclusion in

the New Year Honours List for 1954,

Although he possessed the wide knowledge of biology essential to his posi-

tion as Director of the South Australian Muscum, his deeper interests always

appear to have had an aquatic bias, His earliest writinys concern freshwater lite,

outstanding among which were his studies on aquatic Hemiptera, while his sttb-

sequent rescarch was mainly in marine biology. He will be remembered best for

his work on sonthern Australian Crustaceans. His British Science Guild Hand-

book, “he Crustaceans of South Australia”, published in 1927 {Part 1) and

1929 (Part IL) is now a widely recognised text, while his revisionary studies ou

the Australian Cumacean Fauna provided a new foundation for the taxonomy

of this order. His work has been used extensively by subsequent systematists.

After retiring on the 30th September, 1960, he maintained an active interest

in his investigation of the whale fauna of the Southern Ocean, and added three

papers to his already iinpressive contribution to research in this field. The

manuscript of a further paper was completed just prior to his death, and is now

being prepared for publication.

In addition to the 94 papers which he published under his own name, some

ot his work was undertaken in collaboration with other authors, outstanding of

which were his work with Edgar R, Waite on Lophobranchiate fishes, and his

joint papers with Norman B, Tindale on Australian ethnology and anthropology.

For his outstanding contributions to “research in science” he was awarded

the Verco Medal of this Society at its General Meeting in Jane, 1947.

FM.

LIST OF LECTURES GIVEN AT MEETINGS DURING

THE YEAR 1962-63

Summary

LIST OF LECTURES GIVEN AT MEETINGS DURING

July, 1962,

Aug,, 1962.

Sept., 1962.

Oct., 1962.

Nov., 1962.

April, 1963.

May, 1963,

June, 1963.

THE YEAR 1962-63.

Dr. N. H. Lupsroox: “Correlation of the Tertiary Rocks of South

Australia”.

Dr. R. L. Honce: “Studies on the Peripheral Circulation of Man”.

Mr. K. J. Hurcuinson: “Factors Affecting Wool Production in $.A.”

Dr. C. R. Twware: “Geomorpholgy of the Adelaide District”.

Mr. H. C. Brineson: “Libraries in the Scientific Age”.

Dr. C. R. Jewxiy: “The Host-Parasite Relationship”.

Dr, H. B. §. Womerstey: “Plant Food from the Sea”,

Mr. E. S. O’Driscouy: “The Earth as a Transformed Ellipsoid”.

EXHIBITS

During the year the following members exhibited material at Ordinary

Meetings:

Dr. B. Dan.wv—Lower Cambrian Fossils from Metamorphosed Rocks at Delamere,

Fleurieu Peninsula, S.A.

Mr. F. J. Mrrcurs.r—An example of parallel evolution between two different

genera of gecko lizards.

Mr. M. J. Tyzer—Unusual secondary sexual characteristics exhibited by Hyla

nannotis, a Queensland tree frog.

Mr. M. J. Tytrr—An unusual defensive mechanism in a Leptodactylid frog.

BALANCE SHEET

Summary

ROYAL SOCIETY OF SOUTH AUSI'RALIA (INCORPORATED)

REVENUE ACCOUNT

Receipts and Payments for Year ended 30th June, 1963.

& sg. d. s.

To Balance 1/7/62 289 19 6 By Printing and Publishing Volume 86,

Subseriptions 370 2 8 | Reprints, ete. A . 2,035 13

. Government Grant 1750 0 @Q , Binding and Book Ends 539 4

» Sale of Publications, ete. Lis9 1 40 dy Shelving “ » 133 10

., Kent of Rooms - g: 47 0 0 » Amount Transferred "to Library

., Interest— Account 7 w 8135

Endowment Fund £454 7 4 » Journals, ete. .. 80 5

Bank of Adelaide 31 4 9 » Library Assistants 164 1

.. 2a - 485 12 | » Clerical Assistance 180 1

a » Printing and Stationcry 82 5 |]

£AIBL 15 3 .. Postages and Duty Stamps .. 143 4

4 Cleaning and Polishing 98 0

3 lelephone 1 i 23:10 1

> Insurance .. \ & . 72 843

» Packing and Freight ; 13°11

» Lightme .. . ua 713

nm Addressing Machine 48 15

|, Hire of Key Dises 13 10

. Wreath —- . . 3 0«2

Balance at Bank of Adelaide

LIBRARY ACCOUNT

To Balance . . £313 5 0 Balance at Bank of Adelaide . £313 5

a cr

Audited and found correct.

(Sgd.) F. M, ANGEL

N. $, ANGEL, A.U.A, (Com. )

Adelaide, Ist July, 1963,

Hon.

| F. J. MITCHELL,

{ Auditors

Hon. Treasiver.

ENDOWMENT FUND

‘Transactions for the Year ended 30th June, 1963.

ee a ee se eee

£ +s dd. | & 4s,

To Balance . 9670 0 0 | By Revenue Transfer . 454 7

Tnvestrnent Interest | 4, Balance—

Com’wealth — Tn- | Inscribed. Stock—

scribed Stock .. £434 6 3 | Com ‘wealth £9220 0 0

S.A. Inseribed | South Aust. {50 0 0

Stock — - 410 0 | S.A, Gas Co.

S.A. Gas Co. Bonds 300 0 0

Bonds 15 11 1

——————_ 454 7 4 ————-—— 9,670 0 |

£10,124 7 4 £10,124 7

eee

Audited and found correct, The Commonwealth Stock has been verified by certificate, and the S.A. Stod

and the Gas Co, Bonds have been inspected in the hands of the Treasurcr.

(Sed,) F. M. ANGFI, | Hon.

N. S. ANGEL, A.U.A. (Com.) — f Auditors

Adelaide, Ist July, 1963.

EF. J. MITCHELL,

Hon, Treasurer,

AMENDED LIST OF FELLOWS

Summary

AWARDS OF THE SIR JOSEPH VERCO MEDAL

1929 Pror, Wauren Howon, HGS.

1930) Joun McC. Brack, ALLS.

1931) Pror. Str DoucbLas Mawsex, O.B.E., D.Se,, BE, IRS,

1933 Prov, J, Bowron Ciecann, M.D,

1935 Por. 1. Harvey Jounstos, M.A, D,Se.

1936 Pror, J. A. Prescorr, D.Se,, FAC.

19430 Herseur Wonmnstey, 4.L,5., FIRES,

ltd Pro. J. G. Woon, D.Se., Fh.

1945 Crow TT) Mamean, MLA. BEL, D.Se, F.GS,

1946 Tlenuenr M. Have, O.B.E,

1955 LL. Kerva Wann, 1.$.0., BLA. BE. Dise

1956 N. B, Tinwace, B.Sc.

1957 C. S. Piren, D.Sc.

L960) A. HH. Fint.ayvson,

1961 KR. L. Specut, Ph.D.

1962 H. G. Annrewantua, M.Av.Se,, D.Se.. FAA,

1963 For outstanding: palacontologieu research and contributions to geologien!

chronology in Australia.

N. TL. Gupurook, M.A. PhD. D.C, W.G,8.

LIST OF FELLOWS

AS AT 30th JUNE, 1963

Those marked with an asterisk (*) have contributed papers published in the Societys

Transactions, Those marked with a dagger (1) are Life Members,

Any change in address or any other changes should be notified to the Secretary.

Note.— he publications of the Society are not sent to those members whose subseriptions

are in urrears.

Date of

Date of Honorary Honorary FRu.ows

Election Election

1895 1949 *CcEnanp, Pror. J. B., M.D., Dashwood Road, Beaumont, S.A—Verco Medal,

1933; Council, 1921-26, 1932-37; President, 1927-28, 1940-41; Vice-

President, 1926-27, 1941-42, ;

1913 1955 *Osnorn, Prox. I. C. B., D.Se., 103 Ward Street, North Adcluide—Counceil

1915-20, 1923-24. Vice-President, 1924-25, 1926-27; President, 1925-26.

1912 1955 * Wann, L. K., 18.0. B.A. B.E., D.Sc, 22 Northumberland Street, Heath-

pool, Marryalville, S.A,—Verco Medal, 1955: Canuneil, 1924-27, 1933-35;

Vine-President, 1927-28: President, 1928-30.

1922 1962, *HAtE, AH. ML, O.B.E. 12 Bellevue Phice, Unley. Park, S.A.—Verco. Medal,

1946; Council, 1931-34, 1950-55, 1956-62! Vice-President, 1934-36,

ieee! President, 1936-37: Treasurer, 1938-50, 1953-56: Council,

1957-62.

Date of Fetiow's

Election

1946. *Annre, Prov. A. A.. M.D., D.Se., Ph, Department vf Anitomy, University of

Adelaide, North 'Verrace, Adelaide, S.A.

J961. Amin. C., B.Sc, 42 Kildonan Road. Warradale Park, S.A.

1959. Arrkrn, P., B.Sc,, South Australian Muserm. North Terrace. Adclaide, S.A.

1927, *Arpuiniax, Poor. A. R., Ph.D., DSc, F.GS., Department of Geology. University of

Adelaide, North Terrace, Adelaide, 3.A.—Council, 1937-42., 1954-57; Vice-Presi-

dent, 1962-63.

1961. Anpens, D. J., B.Sc., Dip.Fd., B-Ed., MLA.C.M., c/o. Adelaide Teachers’ College.

Kintore Ayenne, Adelaide, $.A.

1951. *Anpkuson, Mrs, S. H., B.Sc.. 31 Lakeman Strect, North Aculaide, S.A,

1935, “AnpamwartHa, H. G., M.AwSe., D.Sc, BAA, Zoology Dept., University of Adelaide,

North ‘Terrace, Adelaide, SA—Verco Medal, 1962; Council, 1949-50, Vice-Frest-

dent, 1950-51, 1952-535 resident, 1951-52.

255 List OF FELLOWS

Date of

Elechor

1935. "Anprewawas, Mas. HW. G. BoAgr.Se., Mise. (neo H. V, Steele), 29 Claremont

Avenue, Netherby, S.A.

1929, *Ancen, F. M., 34 Fullarton Road, Parkside, S.A.

1939. “Axcen, Miss L. M, M.Se, Zoology Dept, University of Adelaide, North Terrace.

Adelaide, S.A.

L960, ARcHBOLD, HK. ‘T.. South Australian Museum, North ‘Torrace, Adelaide, S.A.

1962. Auvaanr, Mus R. 1, co. South Australian Moseum, North 'forrace, Adeluide, 5.A,

1062, Bacor, P. IL, 62 Hawkers Koad, Medinilie, S.A,

163. Batpock, BR. N., B.Se., 62 Robsurt Street, Parkside, $.4-

1958. _Baurn, FP. H., Department of Geography, University College of Townsyille, Towns-

ville, Queenshenel.

1950, Becx, R. G., B.AgSe., R.D.A., Lynewood Park, Mil-Lel, via Moimt Gambier, 5.A,

1932, Bree, P. R.. D.)0,8c,, L.0.8,. Shell House, 170 North Verrace, Adcluide, S.A,

W238. Brat, BR. J, Se, PAC, Waite Institute (Private Mail Bag, No. 1), Adelaide, 5.A.

1956. Brack, A. B., A.S.A.S.M., M.LM.M., 86 Woodcroft Avende, St. Georges, 5.A,

94. Brack, FO. MB. Bb. Mavill Rowl, Truunere, 5.A,

1962. Bresevc, Mrs, N. M., c/o. Senth Australian Museum, North Terrace, Adelaide, S.A.

1950). saree i. J. MB. B.S., FRACS. (ing), F-B-ACS., 19 Marlborough &t., CQulleve

fark, SoA. ;

1945. ¢°’Boxyrnos, GC. W,, BSe, FRAC, Romulo Honse, Runialo Avenue, Magill, 5.45

Council, T961-.

197. Bowers, D. KR. ELD, (Lend.), DLC, F.G.S5 Departnent of Geology. University,

Glasgow, Scotland.

1957. *Buwoxes, Miss IL. M., Dept. of Entomoloyy, Waite Institute (Private Mail Bag, No.

(), Adelaide, S.A,

1962, Buewn, 2. C., BSc, 3 Jenkins Averme, Myitle Bank, S.A,

161. *Buownen., FL E, Ph.D. e/o. Department of Botany, University of Adelaide,

Adelaicie, §.A,

1957. Buiex, W. G., B.A., c/o Pablic Library, North Terrace, Adelaide, S.A.

M44, *Buusiocr, Miss N.S. M.Se., G.S,.0R.0., Div. Plant Gidustry, P.O. Bax 109, Gan

herra, A-C.T.

1054. Bune, 1, 51 Bichmond Tuad, Westhourne Pyirk, S.A,

1922, *Campnrie, Prov, T, D.. D.DSe., Se, 94 Tynington Street, Tusmore, SA—

Council, 1928-33, J985, 1942-45; Vice-President, 1932-34; President, 1934435.

1960, Casnuer, G., 8 First Avenne, Glewely, S.A,

159. Cannoocs, I. B., R.D.Qem, 26 Denettyille Terrace, Kent Town, 5.4.

1953, Carrex, A. NL, BSc, 8 Seott St, Maroubra Bay, N.S.W

1960, Carrey, D. B.. & Corlmere Terrace, Whyulla, ‘SA

1957, *Cumprenpare, G. M., B.Sc... Lands Avenue, Alive Springs, N.'T.

1955. Chow, B.A, Wydrocleetric Commission, Hobart, Tas.

1949, Cots, VF. S.. Geolory Deparhnent, University of Queensliund, St. Tala, Bris-

pune, O.

1962. Conse. D. W. P., PhD, FG,S., e/o South Aastralion Museum, North ‘Terract,

Adelaide. S.A.

1620, #Corrvos, B.C. BRAS, DP, 166 Wellington Road, Paynebans, S.A. — Council,

1943-46, 145-49, Wie Provident, 1Y49-b0, 1951-52: President, 1950-51; Pro-

ernie Sceretary, VYGH-G2,

1996, Crawroro, A. 1. B.Sc. Mines Department, 169 Thindle St. Adelaide, S.A.

1G. a aed hag ay W, B., MoSe.. DVPhiL, Benth Australian Miyseurn, North Terrace, Ade-

nice, S.A.

1956, Darny, 'B.., Ph.D. Department of Geology, University of Adeliide, North Terrace,

Adelaide. S.A.—Progranume Secretary, 1937-59; Council, TOBHL.

Wos, Davwnson, Ao. C. PAD. B.Su., e/a esses, Simpson & Brookman, 29 Grenfell St,

Adelnicle; S.A.

1930, Unix, E. V., Box 13, Aldyate, S.A. ‘

1957. Donte, K.M., M.AgSe,, Waite Institute (Private Mail Bug, No. 1), Adelaide, S.A.

1963. Duasron, R. 1, BSc. (Hons.), 309 Oaklands Word, Marion, S.A.

1959. Denxnor, &. BR. G., B.Sc. 13 Walton Ave, Clearview, S.A.

1944. Dunsvorn, S. M. L, MLB, B.S., 170 Payneham Road, ‘St. Teters, S.A,

Wal, wre J. MMB, BS. 157 East Terrace, Adeluide, SA, :

North Terrace. Adelaide, $.A—Cuuneil,, 1943-46.

1963. Lens, N.G., 1LO Mitchell Street. Darvin, N-T.

Datc of

Election

1945.

L908,

1962.

LO56.

(960,

TD59.

1927,

1963.

TU51,

1958.

105).

1962,

1962.

1054.

1953,

1935.

1963,

TAGL,

LOG,

LO5Y.

LOA,

tQad,

1949,

LuG62,

1930,

1962.

1046,

1944,

1963,

1960),

1963,

LO58,

1960,

1962,

19dd,

195],

163.

1959,

924,

J04d4.

1047,

1925,

1960.

1945,

198).

1957.

1958,

L963,

TAA.

JOG,

1939.

LISt OF FELLOWS 2no

*Enmtonps, S. ),, BA. PRD. Zoology Departnent, University of Adeluide, North

Terrace, Adelaide. S.A.—Couneil, lW54-35; Propranune Secretary, V55-50

Secretary, 1956-57,

*Enourar, A. G,, 19 Farrell Street, Glenely, S.A—Goimeil, |94 9-53,

*Eowagns. BR. Marion Road, Mariav, SoA

*Kicammn, A, Drasernat., State Merburium, Rotanie Garden, North ‘Verrce, Adehilde,

Fasven, H. W., 15 Auburn Ave. Myrth: Bank, S.A.

Merpper, D. R., B.Se., Dept. of Zoolouy University College: ot Tovensyille, 'Yosvnse

ville, Queensland.

ELON: 47. FL, 305 Ward St, North Adelaide. S.A. Verve Medal, VO60; Council,

937-40.

Tiraran, J. B.. BiSe. (Tons), 1 Wilkins Street, Bast Glenelis, SoA.

Misnun, R. H., 21 Senview Road. Lynton, S.A.

*Fonurs, GB. G,, Ph.D. b.C.8., 9 Flinders Tloud, Hillcrest, S.A.

Pornn, N., Dip,For. C/S.1.R.0., Canberra, A.C.T.

Fusven, R. J. BB. c/o PED, BSP. Serie, Slate of Brunei, Borneo,

Prevrac. 1, B,, Body. 2 Selway Street, Oaklands Park, S.A,

Gissox, A. A, AW.ASM., Mines Depurlinent, 169 Rindlr St., Adelaide, S.A.

°Guarssyen. M, I, Dibe,. FAA. Geolugy Departineni, University of Adelaide,

North Terrace, Adelaide, SA —Counpil, 1953-34; Vier-President, 1958-59,

[Gornsack, H., Coromandel Valley, S.A.

Granra Re 1D, B.Sc, (Hons), eo. Botiny Digartment, University of Adulyide,

North Terrace, Adelaide, S.A.

Green, W. J., B.Se., Delhi Australian Petrolenmn Ltd, 32 Grenfell St, Adelaide, S.A,

Greavity, G.-C. MB, BUS., Medioul Practitioner. Tetuh Grovk, Sut,

Grren. Miss L, M.A. BA. M.Se., Dept. of Anutumy and Histology, University of

Adelaide, North Terrace, Adelaide, S.A.

Gross, G. 1. M.Se., South Australian Museum, Adelaide, S.A—Seeretary, 150-55,

Curry, D. J., BySu. ¢/o W.A. Petrolenm Co,, 251 Adelaide Terrace, Peeth, W.A,

Hart, D. R. Toa Tree Gully, $.A,

Flamiuron-Santy, B., AJA. 17 Helwie Avent. Moulnoreney, Vie

Hlancucn, N. L., 3 Bewdley, 66 Beresford Road, Kese Bay, N.S.W.

Tanne, J. IL, B.Sc, (WAL), 92 East Avenue, Clarence Park, S.A,

“Hanpy, Mus. J. BE, (nec A. G, Beekwith), MSe., Stewart Ave., Salisbury. S.A.

anni, J. T., BySe., c/o Waite Institute {Private Mail Bag, No, 1), Adelaide, S.A,

Hanns, W. K., B-Se., 40 George Skreet, Porreny Park, S.A.

Taiuuson, J., 7 MeQuillan Ave,, Renown Park, S.A,

Mawke, V. L.. MB. B15. 43 Semaphore Road, Semaphore, S.A.

Haynacn, J, F., B.Sc, 68 Pleasant Avert, Clindore, S.A.

Hayman, D. L., Ph.D. Genetiés Department, University of Adelaide, North ‘Terrace,

Adelaide, S.A,

“Mean, G. Ry, BiSe. (Mons), Departuent of Mines, 169 Rundle St, Adelaide, S.A,

Hesrror, R. 1, TeAgeSe.. 49 Halsbury Avenue, Kingswood, S.A.

Hockine, L. J.. 46 Kauri Parade, Seaclill, 3... ;

Hono, KR. LL. MB, BS. MBACP, Departinent uf Physiology. University of

Adelaide, North Terruce, Advkuide, S.A.

Honwirz, RG. H., D.Se., Glenside Road, Woodbury Hill, Stirling West, S.A,

*Hossretp, P.S., Ph.D., 132 Fisher Steeot, Mullurton, $.A.

Toumune, D. 8. W., MubS,, U.P. 256 Payneham Road, Payneham, S.A,

*Hurton, J. t., B.Se., AS ASM. LO Bollewne Plans, Unley Park, S.A. — Council,

1987-61: View-Presidenté LO61-63: Previelent, 1962-63.

Tromp, P., 14 Wyatt Road. Burnside, S.A,

Twenam, L. J. 34 Lexington Road, Munley South, 5.4.

*Teasur, R. W.. MLSe..6 North Perngy Parle, Belair, 5.A.—Cannoil, 1961,

SJouns, R. K., B.Se., Department of Mines, 169 Rundle St. Adelaide, S.A.

JOHNSTON, B., B.Se,Agr., Ph.D,, Waite Institute (Private Mail Bag, No. 1),, Adotaicln,

SwA,

*Jounson, W., B.Sc, (Hons.), 33 Ryan Avenuic, Woodville West, S.A.

Joxrs, J. B.. THD, Gedlogy Department, University of Adelaide, North Terres

Adelaide, S_A,

Keays, A. b., BE. 44 LeWevre Terrace, North Adeliude, S.A,

Kenny, Mus. M.. ¢/o South Australian Musewm, Adelaide, §.A,.

epics Hi, M., Ph.D., M.B., PRGS., Khikhar Buildiags, CP, Tuok Rowl, Boi

aay, India.

ill List OW FELLOWS

Date af

Election

1962. Kuve, Miss M. [. 1.) Mus.Bace.. A.ULA.. “Mirrabooka”, Wilpemt St. deo Hills, S.A.

1949, "Ki~a, D., M-Se. éfo Utah Development Co, Thacr 387A, Tb. & GC. Bidg., Brishane, Q.

1933. *Knenaran, Av W.. Ph.D., Dept, of Geology, University of Adelaide, North Terrace,

Agatti Cy S.A, Seerelary, 1945-48; Vice-Preshtent, V948-49, 1950-51; President,

Ft),

1960, Keonusn, BR, H., Roseworthy Agricultural College, Roseworthy, S.A.

W941, *Lawcwore-Sarerm, T.. BA. Mise, PL, Dept. of Ceography, University of Sydnev,

‘Sydney, NUS.W.

1962, Laws, D. F.. M.A., B.D,. Ph.D.. Zonlogy Dept,, University of Adelaide. Adeliide, 5.4,

1922, Lennon, G. A, M.D., BS. JRC, e/a. Bildes’s. Trustee: and Fxecutor Go. Ltd,

37 Currie Strect, Adelaide, S.A.

1958, Lanvsay, H, A., 110 Cross Road, Highgate. S.A,

148. Loran, T. RON. NOEL UN.Z,). Direetor, Hotanie Garden, Adelaide, S.A—

T peaeetct, 1952-53: Couneil, 1953-57: Viee-Presiident, 1957-38, 1960-61; President,

1955-60).

1991 SLepuneok, Mus. N. H. MLA. PhD, DTC. PGS. Department of Mines, 169

LOG.

164,

19:39,

1959,

1950).

1920),

1965,

14a.

1045,

1962,

(952,

193%.

1938,

I9sI,

1959.

L933,

136,

1957.

S962,

1944,

1962_

1945,

1930,

O56.

1963.

196.3.

1937,

1949,

1920.

{026

1963,

1948.

1925,

Rundle St.. Adelaide, S.A.—Counecil, 1958-60; Vice-President, 19G60-G1; President,

1961-62; Vice-President, 1962-63,

Maenzrn, D, A. Ph.D., Waite Institute (Private Muil Bug, No, 1), Adelaicle, S.A,

Manous. J. efo, South Australian Museum, North Terrace, Adelaide, S.A.

Mansiracr,. T. J., MAgrSe. PHD, G.S.1.8.0., Divistot of Soils (Private Mail Bag,

No. 1), Adelaide, S.A.—Cotnieil, 1945-52. :

*Mfantin, Miss 11. A, ¢/a Department of Botwiy and Biolowy, University of British

Colombia, Vancouver 8, Canada.

Mayo, G, M. BE. BAgSe., hb. 29 Angas Rd., Lower Mitcham, S.A,

Mayo, Sr Tirnurkt, LLB. (.C., 90 Northgate St., Unley Park, S.A.

McBiuan, FE, M., ALSe., University of Adelaide, North Terrace. Adelaide, S.A.

MeCuraotn, RoN., MBE. BSe., BeAueSe,, c/o, Board of Vices Control Box 54,

Lismore, N.S,W.

}* Mines, K, Ri, D.Se., F.G.S.. 1) Chorch Road, Mitelwa, S.A.

Minna, K. J. BSc. 17 Denis Street, St. Murys., SA.

Mionre, K, L,, WG.A., 14 Burlington Strect, Walkerville, S.A.

Mrverranr, V. HL, 30 Wainhouse Street, Torrensville, 5,4,

*Minaws. R. G. B.Su., 5 Myrtle Rel, Seacliff, S.A.

Mircnens, I. J,, South Anstratiun Museum, North. Terrace, Adelaide, S.A —Treasnurer,

1959-,

Mrrereat, Mas. F. J. MSe.. Mraneis Street, Belair, SA,

Mitouerr, Poe’. Sin M. L., M.Se., c/o Elder's Tristee and Ksventor Ca. Luh, 7

Currie Street, Adelaide,

*Mounrroup, GC. 2. 25 Virst Avenue, St. Betars, Adelaide, SA.

“Mim, Ivan. A. B.Sc. (Tlons.), e/o Austrian Atomio Energy Continissi¢n, P.O.

Googee, N.S. W.

Newsome, A. BSe., Animal Cadustey Brunch, N.V. Adniinisttatian, Box 280. Alive

Springs, N,T.

Ninwes. A. KR. BAW R.D.A,, 62 Sheffield Street, Malvern, S.A,

Nixon, L. G. B. BiSe., 38 Sweetwater St, Seacombe Gardens, S.A.

*Norrucorn, K. M., B.AgrSe., ALAS. CSR.O., Division of Soils (Private Mail

Baz, Ne, 1), Adelide, $.A.

Ockesmey, CG. P., BLA. G8 Tolbrooks Rd, Flinders, Park, S.A,

O'Dinscoir, E. §., BSc 9 Vinall Street, Dover Gardens, S.A,

PO, BR. BSe. CHons.), Genlogy Department, University al Adolatde, North

Termee, Adelaide, SiA.

Ouiven, RL. PHD, Geglogy Department, University of Adelaide, North ‘Lorruce,

Adelaicle, S.A.

*Pangas., L, W., M.Sc. AS-T.C., Department of Mines, 169 Rundle St, Adelaide,

S.A.—Secretory, 1953-56; Viee-President, 1956-97, 1938-50; President, 1957-58.

Pansixson, K. J., B.S0., OL Stuert St. Hillerest, $.A,

Paurt, A. G., M.A, B.Sc., £0 Milton Avenue, Fillarton Estate, 5.4,

Comneil, 041-43; Viee-President. 1943-45, LUAG-7, President, 1945-46.

Pootaxs, M, G., MLA. PhD. 12 Mrancls Avene, Pithierton, S.A.

Pownm, J. K., Be. Waite Institute (Private Mall Bag, No. 1), Adelaide, 5.4,

*Pauscort, Puor. J. A. CALE, DSc. FRAC, #.R AS. PAA 820 Cross Rel,

Myrtle Bank, S:A.—Vereu Medal, 1938: Council, 1927-30, 1935-39: Vice-President,

3930-32; President, 1932-33: Rdifor, 1955-68; Connell, 1962-63.

LIST OF PETLOWS 2h]

Date of

Blecuian

1961, Piagry, G. L., BAL, evo South Australian Museam, Adelaide, S.A.

1957. “Piunciue, Mags 1 As B.. Box 8766. G.P.0,, Adelaide, S.A.

1945. *Prvon, L. D. M.se., Dip,For,, 82 La Perouse Strect, Grillith, Canberra, A.C,T

1950, *Rarricaaw, J, Wi, Misec.. Naweustle University College, Tigh’s Hill, 2N, NSW.

14, Kicrman, D, §., D.Sc, BA se, C.S.LR.0., Division of Blochemistry, Adelate, SA.

1947, reper, W. B, BiSu, c/o Seripps Institution of Oemmoyraphy, Dept. of Palacun-

tology, University of California, La Jolla, Galitornia, U.S.A.

1963, Rosseysan, Praae KOON, FBS. FAA. DSc, Ph.D. (Camb.), Deparkinent of

Botuny, University af Adelaide, Narth Terrace, Adelaide, S.A.

LO53, hocens, Pune, W. P., D.Se,, PhD, FAA, M.I,Bial., Zoology Dept., University of

Adelaide, North Terrace, Adelaide, S.A,

L951, Rowe, &. A. 22 Shelley Street, Firle, S.A.

195), Kup, Prov, be A. Base, AML, University of Adelaide, North Terrace, Arlelaide,

S.A.

195]. Russece, L, D., c/o Adelaide Bays’ Aish School, West Terrace, Adelaide. SA,

16.3. Hessuuc, R. EL, MOB. BS.. MURLALC.PL 267 Praetrush Road, Clenunes, S.A,

1945, Hynucy, J. IL, Old Penola Mstate, Ponala, 5,A,

1933, Scmyminen, ML. MAB. B.S. 175 North Terrace, Adelaide, S.A.

1859, FORCED Fe, Division of Land Research and Divisional Survey, C.S.LB.0., Caa-

berra, ACA,

$951, PS8earr, TD. M.Se, Western Teachers’ College, Taylors Rel, Thebarton, S$ A—

Progrumme Seerctary, 1953-54, 1956-57; Secretary, L957-.

1925. °Sneano, H., Port Elliot, S.A.

1936, "SHeanp, Ky D.Sc, 19 Webster St. Nedlands, W.A.

1954. Srepnenn, AG. B.Se.. o/o Department of Mines, 169 Rundle St, Adelaide, S.A

(961. Stmmimin, SAL BVA. LLB. 5 Rosevear St, Hawthorn, $.A,

1934, Swinkrfenn, R, C., 57 Canterbury Avenue, Trinity Gardens, S.A.

162. Sarane, D., M.Se., c/o Dopartwonl of Mmes, Rundle St, Adelaide, S.A.

1025. {Sauni, Sik Toar Barn, Kt, B.A,, 24 Crrrie Street, Adelaide, S.A,

IW4h *Sauracorr, R. V., MD, H.5., D.T.M. & TL, 13 Jasper Strevt, Hyde Park, $.A—

Council, (49-51, 1952-53, LOBT-GO. Wieeserer, 1951-52, Vice-President, 1953-54,

1955-A6, ING1-62; President, 1954-55, TOBN-6I.

TH47, “Serco KR. L.. PhD. Botany Departinent, University of Melbourne—Verco Meal,

cd Gojeneil, 1931-52, 1958-60; Programme Seerctary, W52-33; Vice-Previdynt,

16).

1936. { "Space, Ry C. Mibe. 6 Baker Street, Somerton Park, S.A,

1949, *Seyy, A. IL, M.Sc, Geolagy Departnent, University of Tasmania, Hobart, Tas.

1951. SrrApsan, Rey. W. RR. 8 Blairgowrie Road, St, Georges, 5.A.

US, “Srernens, C. G., D.Sc, C.S..8,0., Division of Soils (Private Mail Bag, No, 1), Arle-

laide, S.A—Verco Merlal, 1959; Council, 1952-54; Vice-President, 1954-55, 1956-

57; President. 1955-56,

1955, Swaine, C. DB, MT, B.S., 220 Esplansde, Largs North, S.A,

LG Swinnounng, BH. F.C. Box 210, P.O., Alioe Springs, N.T.

151. Swinses, Py, MLAwSe., 13 Derwent Ave. Kostrevor, 5A.

ING2. "Symos, D, E., BoAgSe., Waite Institute (Private Mail Bag, No. 1), Adelaide, S.A,

NBO, Syatews, Wh. I, Uraainnt Treatment Plart, Port Pirie, S.A.

1934. pee ag L.G., 85 Minray Street, Lower Mitcham, §.A.—Editor, 1947-55; Council,

SS.

W633, “Taynor, J. bo MA, PhD. University of Adelaide, North ‘Terrace, Adelaide, $.A,

1958. TAO, a J), Dept. of Entomology, Waite Institutes (Private Mail Bag, No. L),

Adelaide, S.A.

194, Tavnan. D, J... 23 Westbourns St, Prahran East, Vic.

2d. *TarLton. J. B.. BA. AESe., BoSeAgr, O.S.L8,0., Division Of Soils (Private Mull

Bay, No, 1), Adelaide, S.A,\—Conneil, 1940-49, 1947-50: Librurtim, 1051-52: View

President, 1952-35, 1954-55; President, 1953-54; Editor, LOAe-

W961, Teague, Ff. A., e/o@ Post Offive, Howker, §.A,

1962, Teusnen, BR. E., LL.B. o/o. Post Offiee, Tanunda, S.A,

148. °Tronas, 1. Mi, M.Se. (Wales), Mi[Biol. Department of Zoology, University af

Adelaide, S.A.—Secrefary, 1945-50; Council, 1950-53; Viec-President, 1955-56,

1957-58: President, 1956-57; Assistant Editor, 1958-.

(958, °Trroytas, Mus. 1M. (nee P, My Mawson), M-Se.. Departinent af Zoology, University

of Advlaitle, North Terrave, Adeluide, S.A.

1957. Tomas, J., B.Sc., Woodleigh Road, Blackwood, $ A-

1959, Tomson, B. P., M.Sc, 33 Oaklands Road, Parkholme, S.A.

1940, *Tomson, Carr. J. M., 185 Military Roacl, Semaphore South, SA.

962

Date of

Election

1923,

1955.

1959.

1960.

1950.

1953,

1954.

1954,

1959,

1962,

1946,

1950.

1946,

1961,

1954,

1944,

1957,

1960).

1949,

1944,

LIST OF FELLOWS

*Ty~patz, N. B,, B,Sc., South Australian Museum, North Terrace, Adelaide, $.A.—

Verco Medal, 1956; Secretary, 1935-36; Council, 1946-47; Vice-President, 1947-

48, 1949-50; President, 1948-49; Librarian, 1952-.

*Tucker, B. M., B.A., B.Sc,, C.S.LR.0O., Division of Soils (Private Mail Bag, Na. 1),

Adelaide, S.A.

Twma.e, C. R., Ph.D., M.Se., Dept, of Geography, University of Adelaide, North

‘Terrace, Adelaide, S.A.

*Tyier, M. J., Dept. of Physiology, University of Adelaide, North Terrace, Adelaide,

S,A.—Programme Secretary, 1962-.

Tynan, A. a c/o Australian Mineral Devyclopment Lahoratorics, Flemington St.,

Parkside, S.A.

Verrcu, J. T., Box 92, Port Lincoln, S.A.

WatTeRMAN, R. A., B.A. M.A., Ph.D., Wayne State University, Detroit, Michigan,

ULS,A.

*Wiss, B. P., M.Sc., Department of Mines, 169 Rundle St., Adelaide, S.A.

Wetts, GC. B., M.Ag.Sc,, Broadlees, Waverley Ridge, Crafers, S.A.

Wut tan, Pror. R. F., M.D., Ph.D., D.Sc., Department of Physiology, University of

Adelaide, North Terracc, Adelaide, S.A.

Wuirten, G. F., B.Sc., c/o Department of Mines, Rundle Street, Adelaide, S.A,

°Waurrtie, A, W. G., M.Se., Department of Economie Geology, University of Adelaide,

North Terrace, ‘Adelaide, S.A.

Wiu1ams, L, D., “Dumosa,” Meningie, S.A,

°Wirson, Pror. A. F., D.Sc., Dept. of Geology, University of Qucensland, St, Lucia,

Brisbane, Qld.

°"Winson, P. G., B.Sc., c/o Botanic Garden, North Terrace, Adelaide, S.A.

*Womenrstey, H. B. §., D.Sc., Botany Department, University of Adelaide, North ‘Ter-

Adelaide, $.A.—Council, 1960-.

Womens.ey, J. S,, B.Sc., Dept. of Forests, Lae, New Guinea.

Woops, R, V., B.Sc., Mt. Crawford, S.A.

*Worrner, H., Ph.D., 16 Reece Ave., Klemzig, S.A.

Yrares, J. N., A.M.LE., A.M.I.M-E., Highways and Local Government Dept.,

Adclaide, S.A.

Zimmer, W. J., Dip.For., F.L.S8. (Lond.), 7 Rupert St., Footscray West, W,12, Vic.

NEW SPECIES AND VARIETIES DESCRIBED IN THIS VOLUME

Summary

263

NEW SPECIES AND VARIETIES DESCRIBED IN THIS VOLUME

Listriolobus bulbocaudatus — - - - : - - 243

Millotia greevesti var. glandulosa - - - - - 222

Millotia macrocarpa — - - - - - - - 228

Millotia tenuifolia var. nudescens - - - - - 234

Ochetostoma myersi — - - - - - - - 245

Trichosurus vulpecula raui_ - - - - - - 18

CONTENTS

N. H. Lupsroox: Correlations of the Tertiary Rocks of Australia - -

H. H. Fintayson: The Brush- aed Cpa oS ee eae Sau:

Australia - - - -

C. H. 8. Warrs: Larvae of Australian Dytiscidae (Coleoptera) - -

J. N. Jennincs: Some Geomorphological Problems of the Nullarbor Plain

R. L. Specur (with J. B. CLeLanp): Flora Conservation in South Australia.

Part II. The Preservation of Species Recorded in South Australia -

D. F. Smrru: Plant Ecology of Lower Eyre Peninsula, South Australia -

J, A. Mumme: Geophysical Survey of the Officer Basin, South Australia -

R. Crawrorp: The Wooltana Volcanic Belt, South Australia - - -

H, W. Fanner: The Wooltana Lavas - - - - - ~ -

G. R. Hearn: Stonyfell Quartzite: Tesauete Siralseray hy) ae Peas

graphy of the Type Section = -

Kinestey J. Mixxs: Structural Geology of the Mt. Crawford Granite Gneiss

and Adjacent Metasediments - ~ : : : P 7 =

J. L. Tasor: SERS Die BEST Sk the peouehiton Ramee, oo

Australia - .

I. A. Mumme: Crustal Thickness in the Maralinga Area, South Australia -

R. Orrcter: Structural Seology. of ths sure Hg. BGeehne, Sgn

Australia - - - -

R. SceoppE: Taxonomic Revision of the Genus Millotia Cassini - -

S. J. Epmonps: Two New Echiuroids (Echiuroidea) from Australia - -

Obituaries:

Herbert Womersley, A.L.S., F.R.E.S. - 3 2 2 z E E

Charles Mervyn Deland, M.B., B.S., D.P.H., D.T.M. - - - -

Herbert Mathew Hale, O.B.E. - : = z : z re

List of Lectures and Exhibits - - “ : : - a

Balance Sheet - : ; = : L . . - f

Award of Verco Medal - - - - : - : - 3 :

Amended List of Fellows - : = x < 2 = - !

New Species and Varieties Described in this Volume ~ - = =