VOL. 102, PARTS 1 & 2 28 FEBRUARY, 1978

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Wollasten, Eiise M. Two new species of Platythamnion J. Agardh (Ceramiaceae,

Rhodophyta) from Eastern and Southern Australia - - - 1

Smaies, Lesley R. & Mawson, Patricia M. Nematode parasites of the Kangaroo

Island Wallaby, Macropus eugenii (Desmarest). 1. Seasonal

and geographical distribution - - - - - 2 - 9

Tyler, M. J., Davies, Margaret & King, Max. The Australian frog Chiroleptes

dahlii Boulenger: its systematic position, morphology, chromo-

somes and distribution - - - - - - - - 17

Piummer, P.§. Stratigraphy of the lower Wilpena Group (ate a

Flinders Ranges, South Australia - - 25

Fatchen, T. J. Change in grazed Atriplex vesicaria and Kochia astrotricha

(Chenopodiaceae) populations, 1929-1974 - - - - 39

Berry, R. F., Flint, R. B. & Grady, A. E. Deformation history of the Outalpa

area and its application to the Olary Province, South Australia 43

Brittan, N. H.. A new species of Thysanotus R.Br. (Liliaceae) from Eyre Pen-

insula, South Australia - - - - = - - - 55

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

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NORTH TERRACE, ADELAIDE, S.A. 5000

TRANSACTIONS OF THE

ROYAL SOCIETY OF SOUTH AUSTRALIA INC.

CONTENTS, VOL. 102, 1978

PARTS 1 & 2, 28 FEBRUARY

Wollaston, Elise M. Two new species of Platythamnion J, Agardh (Ceramiaceae,

Rhodophyta) from Eastern and Southern Australia - - -

Smales, Lesley R. & Mawson, Patricia M. Nematode parasites of the Kangaroo

Island Wallaby, Macropus eugenii (Desmarest). 1. Seasonal

and geographical distribution - ~ - - - - -

Tyler, M. J., Davies, Margaret & King, Max. The Australian frog Chiroleptes

dahlii Boulenger: its systematic position, morphology, chromo-

somes and distribution - - - - - - - -

Plummer, P. S. Stratigraphy of the lower Wilpena Group (late Precambrian),

Flinders Ranges, South Australia - - . - - -

Fatchen, T. J. Change in grazed Atriplex vesicaria and Kochia astrotricha

(Chenopodiaceae) populations, 1929-1974 - - - <

Berry, R. F., Flint, R. B. & Grady, A. E. Deformation history of the Outalpa

area and its application to the Olary Province, South Australia -

Brittan, N. H. A new species of Thysanotus R.Br. (Liliaceae) from Eyre Pen-

insula, South Australia - - - - - - - -

PARTS 3 & 4, 31 MAY

Robinson, J. F., Robinson, A. C., Watts, C. H. S. & Baverstock, P. R. Notes on

rodents and their ectoparasites collected in Australia in 1974-75

Milton, B. E. & Twidale, C. R. Structure of the Willochra Basin, southern Flinders

Ranges, South Australia - - - “ = z 4

Smales, Lesley R. & Mawson, Patricia M. Nematode and other helminth parasites

of the Kangaroo Island Wallaby. Macropus eugenii (Desmarest).

2. Site selection within the stomach - - - - - -

Bye, J. A. T., Dillon, P. J., Vandenberg, J. C. & Will, G. D. BaLay One of Lake

Eyre - - - . - - :

Tetzlaff, G. & Bye, J. A. T. Water balance of Lake Eyre for the flooded patie

January 1974-June 1976 - - - - -

Roberts, J. D. Redefinition of the Australian epiodactyi frog Neobatrachus

pictus Peters - - - - - : 2 ™ a

Duihunty, J. A. Salt transfers between North and South Lake Eyre - - -

Mawson, Patricia M. Macropicola ocydromi n.g., n.sp. (Nematoda: Strongylidae)

from a Western Australian kangaroo - - - = “i

PARTS 5 & 6, 31 AUGUST

Grubb, E. A. A. Stratigraphy, palynology and implications of organic bands in a

small quaternary basin, near Palmer, South Australia - -

Sheard, M. J. Geological history of the Mount Gambier Volcanic Complex,

southeast South Australia - - 2 : 2 . 2

Daly, S., Webb, A. W. & Whitehead, S. G. Archaean to early Proterozoic banded

iron formations in the Tarcoola region, South Australia - -

Tyler, M. J., Davies, M. & Martin, A. A. A new species of om frog from the

Northern Territory - - - - : = =

Van Deur, W. J. Earthflows in the Yankalilla area of South Australia: significance

of rainfall, soil properties and Man’s activities - = : -

Hails, J. R. & Gostin, V. A. Stranded shingle beach ridges, upper Spencer Gulf,

South Australia: evidence for high wave energy dissipation

during the late Pleistocene - - - - - - -

PARTS 7 & 8, 30 NOVEMBER

McKenzie, K. G. Ostracoda (Crustacea: Podocopida) from southern Australian

salt lakes, with the description of Reticypris new genus - -

Parker, S. A. & Cox, J. B. Notes on the birds of Pearson, Dorothee and Regeaty

Islands, South Australia - 2 a & = F

Flint, D. J. Deep sea fan sedimentation of the Kanmantoo Group,

Kangaroo Island - - - : 2 : 2 s

Mawson, Patricia M. A new genus Adelonema (Nematoda: Oxyuridae) from

Australian phalangerid marsupials - - - - -

Annual Report of Council - - - - : 2 . 2 : a

Award of the Sir Joseph Verco Medal -'— - - - : : 3 =

Balance Sheet a. ~ 2 = _ m= 2 ~ = : 4 a

169

175

191

203

223

227

228

229

TWO NEW SPECIES OF PLATYTHAMNION J. AGARDH

(CERAMIACEAE, RHODOPHYTA) FROM EASTERN AND SOUTHERN

AUSTRALIA

BY ELISE M. WOLLASTON

Summary

Two new species, Platyhamnion cuspidatum and P. francisianum, are described from eastern and

southern coasts of Australia. Both are small, uncorticated plants characteristic of the genus

Platythamnion J. Agardh, with whorls of 4 (2 long and 2 short) adaxially branched whorl-branchlets

on each axial cell of the thallus.

TWO NEW SPECIES OF PLATYTHAMNION J. AGARDH (CERAMIACEAE,

RHODOPHYTA) FROM EASTERN AND SOUTHERN AUSTRALIA

hy Exise M, WoLLaston*

Summary

Wo Lcaston, E. M, (1978) ‘Two new species of Platythamnion 1, Agardh (Ceramiaceae, Rhodo-

phyta) from eastern snd southern Australia, Trans. R, Sec. 8. Aust, 102(1), 1-7, 28

February, 1978.

Two new species, Plaiviammion cuspidataum and P franelsianum, are described from

eastern and southern coasts of Australia. Both are small, uncorticated plants characteristic of

the genus Platythamnion J, Agurdh, with whorls of 4 (2 long und 2 short) adaxially branched

whorl-branchlets on each uxial cell of the thallus.

Introduction

J. Agurdh (1892) first described the genus

Plarythamnion based mainly upon Callitham-

nion heteramerphum J.Ag. (type loeality,

Santa Cruz, California), Since that time fur-

ther species have been recorded from the west

coast of North America (Kylin 1925,

Wollaston 1972), Japan (Inagaki 1935,

Vokida & Inaba 1950), New Zealand (Adams

ef al, 1974) and one, P. nediferum (J,Ag)

Wollaston from southern Australia (Wollaston

1968). P. nediferum which occurs commonly

on coasts of southern Australia is a large plant

(lo 20 cm high) with axes densely corticated

in the lower parts with rhizoidal filaments.

Plaiythamnion cuspidatum sp. nov, and P.

francisiunum sp. nov, represent the — first

records from Australia of uncerticated species

of Platythamnion I.Ag. similar in habit to

those occurring on the Pacific coust of Nerth

America and in Japan,

In all previously described species of Platy-

thamnion the position, form and development

ol carpogonial branches and carposporophyte

are markedly similar, and are typical of the

wibe Antithamnicac, Hence segregation of

taxa within the tribe is based primarily upon

vegetative features and, on this basis, species

ol Platythamnien torm a well-defined generic

group (Wollaston 1972),

Recently liquid preserved material of the

two species described below has become avail-

able for study and although stages of carpo-

sporophyte development are lacking, the plants

are readily recognized as spectes of Plery-

thamnion and described on the basis of vege-

tutive and tetrasporangial features, All

measurements quoted are taken within” the

gelatinous sheath which covers the thallus.

Terminology follows Wollaston (1968), Type

specimens hive been deposited in the Her-

barium of the Department of Botany, Uni-

versity of Adelaide (ADU).

Identification of the genus

Sexual reproduction in Platythanimion has

been described in detail by Wollaston (1968,

1972). However, tetrasporangial features arc

less consistent, and position of tetrasporangia

of inner cells of whorl-branchlets has been

used with vegetative features fo distinguish

species of the genus (Wollaston 1972).

The genus is most readily recognized by the

form und arrangement of whorl-branchlets

which occur in whorls of 4 |2 opposite long

(major) whorl-branehlets at right angles to 2

opposite shorter (minor) whorl-branchlcts]

from cach axial cell, and the pattern of deve-

lopment at growing branch apices,

Major whorl-branchlets are typically oppo-

sitely or adaxially branched from a_ distinct

rachis and ure arranged distichously on branch

axes so that thallus branches appear to be

flattened laterally (Figs 15, 18). In some spe-

cies, two branches occur side by side from

inner cells of whorl-branchlet rachides (Fig.

= Department of Botany, University of Adelaide, North Terrace, Adelaide, S. Aust. 5000.

CAG,

C | J

Xi C

O JOOS 50

ELISE M. WOLLASTON

NEW SPECIES OF PLATYTHAMNION (RHODOHYVPTA) 3

10), The arrangement of these branches and

of further branches developed from them,

furm the basis of species segregation,

Minor Whorl-branchlets are never as con

splenous nor as rewulucly branched as major

whoarl-branehlers and io Australian species

(including P, nediferum) are unbranched or

wilh I-several short branches arising fron) a

short rachis (Figs 2-6, 11). Wollaston (1972)

deseribed an enlarged rounded basal cell bear-

ing usually three short branvhes for four ol

the five Pacific North American species. To-

winds the base of the plant, whorl-brarichlets

may beeame more densely branched or ure

sometimes reduecd in length und branching

Thus the form of Whorlhranchlets in. the

lower thalluy may help in species identitica-

tion,

Lateral thallus branches are formed in place

ol whorlbeanvblets in distichous. alternate

sequence at intervals of several (usually 4-10)

axial cells, and near branch apices they con-

Inihute to the distinetive pattern of axial deve.

lopment. Young lateral branches develop

rapidly and grow up to overtop the axial apex

whieh ts deflected away from the young lateral

(Figs 13, (9), Whorl-branechlets clongate

much more slowly and are offen suppressed

in development along the inner side of un axis

lying Closely adjacent to another branch (Fig.

13), Thus during varly development whorl-

hraneblets are often small or completely lack-

ing from the inner side of young lateral

hranches and fron) primary axes themselves

Deflection of branch axes away from futerul

hrinehes during development often produces

a pseudodichotomous pattern of — thallus

branching throughout the plant (Fig. 15),

Glind vells ure developed laterally on cells

of the ruchis or branches of whorl-branchlets

(Figs 3, t4) and are scattered, sometimes

abundantly, aver the thallus

Key to Anstralian species of Plaiy/lanunion

1. Plant lure, to 20 cm high, lower axes slenscly

corticated with rhizoidal filaments

P, nadilerun {T.Ag.) Well

1, Plant small, ta 2 cm high, completely becking

rhvoidul vortiestion 2

2. Major whotl-branchlets adaxially brinched

wilh it sinule row ef branches which are

themselves branched fram the outer side,

Minor = whorl-branehlets with — spine-like

branches P, cispidarim sp. "OV.

2. Major whorbbrinchlets udaxially branghed

with hranches whieh wsially geeur im pairs

from inner rachis cells und ure themselves

biunched from the Inner side Minor wharl-

branchlels simple or with | to severi) short

branches, , francisianum sp. may.

Vhatythamnion cuspidatam sp, nov.

(FEGS 1-4, 15-17)

Thallis 11-2) em high consisting of

brunehed axes without rhizdidal cortication;

each Wxial cell bearing 2 uppasite loug (major)

whorl-branchlets al right angles ta 2 opposite

short (minor) whorl-branchiets, Majiur whorl-

branchlets to 250 ym long, branehed from the

udaxial side of rachis With abruptly tapered

ycute branches, to 100 pm long, which often

bear further short branches from the outer

side; minor Whorl-branehlets simple or

branched, to 130 pm long, often with 3(-4)

tapering, actite spine-like branches, Gland

cells lateral on cells of whorl-branchlets.

Curposporophytes terminal on branches. Sper-

Mmatangia forming dense clusters on cells of

Whorkbranchlet branches, Tetrusporangia on

cells of whorl-branchlet branches, sessile,

spherical, to 30 ym diameter, erucitely-

divided but often appearing tetrahedral.

Thallus ad 2 cm ullus; axes sine corticatione

rhizoideorum, Omnis cellula oxtalis ferens 2

ramulos verticillorum Maiores oppositos et 2

rumulos verticillarum. minores oppositos ad

angulum 9O° patentes, Ramuli verticdlorum

miiores ad 250 ym longi, in Jatere adaxiali

Figs | 9, MMatyrthanmion euspidutum,

Vig. ! Form of major whorl-branchlet (diagreammanue).

Figs 2-6. Forms of minor whorl-branchlets, with spine-like processes shown in figires 5 and 6 and

presence of a gland-cell in figure 3,

Fig. 7. Spermatangia developing on cells of whorl-hranchlet branches,

Fig. &. Sperroulaogial clusters on whorl-branchlet branches.

Fig, 9, Tetrusporungia orm cells of whorl-branchlet branches.

Figs 10-14, Meayrthunnion francisianumn.

Fip. 1). Form of major whorl-breanchlet (diagrammatic )-

Fiz. (1. Form of minor whorl-branchlet bearing short branches (diagrummuaue )-

Fig. 12. Form of whorl-branchlets towards base of thullus (diugrammutic).

Hig, 13. Development of branch apex showing branch axis (a) with lateral branches |) qnd loo and

whorl-branchlets developing Goly from abaxial side of |).

Fig. 4, Telrasporangia developed on cells of whorl-branchlet branches; a pair of branches one of

which bears a gland cell, is shown on the second cell of the rachis.

4 ELISE M. WOLLASTON

Figs 15-17. Platythamnion cuspidatum.

Fig. 15. Portion of laterally flattened thallus showing whorl-branchlet form and pseudodichotomous

branching of axes.

Fig. 16. Spine-like branches of minor whorl-branchlets.

Fig. 17. Tetrasporangia on branches of major whorl-branchlets.

NEW SPECIES OF PLATYTHAMNION (RHODOHYPTA) 5

Figs 18-19. Platythamnion francisianum.

Fig.

branch (right).

rachidi, ramulis secundariis peracutis ramosi,

ad 100 ym longi, gerentibus plures ramulos

breves externe; minores ramuli verticillorum

simplices vel ramosi ad 130 ym longi, saepe

3(-4) ramulos gradatim acutos spinulosis

gerentes. Cellulae glandulosae in lateribus

ramulorum verticillorum. Carposporophyti in

ramulis terminalia. Spermatangia botryoidea in

cellulis ramulorum verticillorum orta. Tetra-

sporangia sessilia, globosa, ad 30 ,»m diam.,

cruciatim sed in facie saepe tetraedrice in cel-

lulis ramulorum verticillorum portata.

The species is named for the spine-like

branches developed on minor whorl-branch-

lets.

Type locality: Port Kembla, N.S.W., about

20 m deep (J. Watson, 16.ix.1976).

Holotype: ADU, A47994,

Distribution: Known from the type locality

and from Gabo I., Victoria (Shepherd,

19.11.1973). Growing on the mussel Tri-

choma hirsuta, on hydrozoans and on other

algae.

18. Portion of a laterally flattened thallus showing whorl-branchlet form.

19. Tetrasporangia on whorl-branchlet branches (left), and early stage in development of lateral

Platythamnion cuspidatum is distinguished

by the branching pattern of the whorl-branch-

lets. Major whorl-branchlets are branched

adaxially from cells of the rachis with

branches which taper abruptly to an acute

point and which bear further short branches

from their outer side (Figs 1, 15). Major

whorl-branchlets are widely spaced and sel-

dom extend to adjacent whorl-branchlets

above. Where a lateral branch is formed in

place of a major whorl-branchlet, the opposite

major whorl-branchlet often remains short and

unbranched. Minor whorl-branchlets may be

unbranched or with 1l-several simple branches

(Figs 2-4), but are frequently distinctive in

bearing 3(—4) narrow, tapered, acute spine-

like branches which develop from the upper

end of a short 2-celled axis (Figs 5—6, 16);

occasionally this branch axis is extended and

may bear further “spines”, or may itself be-

come spine-like. Axial growth occurs as

typical for the genus and mature axial cells

have an average length to breadth proportion

of 5:2, up to 150 pm long and 60 »m broad

t ELISE M. WOLLASTON

in central parts of thallus. bul are vsually

shorter an proportion to length at the base of

The plane.

Rounded groups of carpusporangia occur

near branch wpices; however, stages ol carpo

spurophyle development have not been avail

ible tor study,

Spermatangia are horne trom the upper part

of cells of whorl-branchlet branches which

arise from immer and central cells ef whorl-

branchlet tachules. A single spermatangium

develops first followed by further sperma-

langial cells (Fig. 7). So that up te four

Matlire apermulangta may be present on a

sinule cell at Oe time, Dense spermatangial

Clusters are thus formed (Fig. &),

Tetrasporangia ate also formed trom the

upper end of cells of whorl-hranchlet

hranches. bul ure confined to inner branches

which are sotietimes only Z-severil cells long

(Wigs 8 17),

Plievihamnion euspidatin is applirently

jolerwat of pollyted water and very low light

vonditions At Port Kembla, N.S.W., if occurs

on depauiperate reefs subject to regular inun-

dations of ipon-rich Nae [Pe(OH).] with con-

sequent low light mtensity (J. Watson, pers.

comm. |

Platythamnlon francisianum sp. nov.

(FIGS 10-14, 18-19)

Phallus to | em high consisting of branched

axes withowl rhizdidal corticution; ¢ach axial

ecll hearing 2 opposite long tmajor) whorl-

franchlets at right angles to 2 opposite short

(miner) whorl-branehlets. Major whorl-

branchlets (o SOO jum long, branched from the

adaxial side of the rachis with branches lo

200 jam long which usually occur in pairs

from inner cells of the rachis and often over-

lap The adjacent whorl-branchlet above, These

branches themselves bear further narrow,

tapering branches from the inner side. Minor

whorl-branchlets to 175(-200) pm Jong,

simple or branched with [several simple

hranches. Gland cells lateral on cells of whorl-

branchlets. Procarp, carposporophyte and

spermatangia unknown, Tetrasporangia of

cells of whorl-branchlet branches, sessile, sub-

spherical, to 36 pm in diameter, cruciately-

divided but often appearing tetrahedral.

Thallus ad | cm alttis; axes ramosi sine

eoricatione rhizoideorum: omnis cellula axi-

alis ferens 2 ramulos verticillorum muatores

oppositos et 2 ramulos verticillorum minores

ad angullim 90° patentes, Ramuli verticillorum

mirores al SOQ jut longi am latere adaxiali

rachidi ramulos secundarios ferentes ad 200

pi longes sacpe binatin: ex interioribus cel-

Wihis rachis el saepe super ramulum verticil>

laruin conliguum superum superpositos. Ra-

Muli secundarii plures ramulos gradatim

decrescentes terunl, Ramulr -verticillorum

minores ad 175(-200) ym longi simplices vel

famosi cum une aliquotue simplicihus ramu-

lis, Cellulae glaundulosae in lateribus ramu-

forum verticijlorum Procarpium et carpo-

sporophylum ct spermalangia ignotu, “Tetra-

sporangia sessilia, subglobosa, ad 36 wm diam.,

cruciatim sed in facie sacpe tetraedrice in cel-

lulis ramutorum verticillorum portata,

The species is named for the type locality.

Type locality: St Francs L.. Isles of St Pran-

cis, S. Aust., S-W face, 55 m deep (Whep-

herd, 94. [97|)

fMolorype: ADU, A3S087,

Djstethytion: Known only from the type loca-

lity, growing on Ballla prariata Harvey,

Playthamnion francisianum is distinguished

by the form of its whorl-branchlets. Major

whorl-branchlets are branched adaxally from

cells of the rachides with branches which often

accur i pairs on each inner rachis cell [Figs

10, 14); these branches are further branched

from the inner side, but sometimes appear as

if subdichotomausly branched (Fig, 10),

Mature whorl-branchlet branches are narrow

and gradually tapered to an acute point (Fig.

18). Towards the base of the plint whorl

branchlets are shorter (-200 pm long) and

more densely branched than those above (Fig

12). Minor wWhorl-branchlets are simple or

with |—several short branches (Fig. 11),

Axial growth oecurs as typical for the genus

and axial apices are overtopped by developing

lateral branches and whorl-branchlets (Pigs

13, 19), Mature axial eells have an average

length lo breadth proportion of 3:2. (up to

200 ym tong and 130 jm broad) im central

parts of the thallus, but are often somewhat

longer in proportion to breadth at the base of

the plant.

Tetrasporangit wre borne from lower cells

of inner and central branches of whorl-hranct

Jets, but are often lacking or Jess numerous

on branches borne on the basal cells of

rachides (Figs 14, 19).

Although this species is known only fron

a single collection jt appears to be clearly

distinct, Frrther details of reproduction and

Variauow in form await future collections.

NEW SPECIES OF PLATYTHAMNION (RHODOHYPTA) L

Acknowledgments

I am grateful to Mr S. A. Shepherd for

Latin diagnoses and to others who have con-

tributed to this study, and particularly for

technical assistance provided through a grant

from the Australian Research Grants Com-

mittee.

References

ADAMS, N, M., Conway, E, & Norris, R. E. in

association with E. A. Wr_ia of Stewart

Island (1974) The marine algae of Stewart

rey Rec. Dom, Mus., Wellington 8(14),

185-245.

Acarpu, J. G. (1892) Analecta algologica. Acta

Univ. lund, 28, 1-182, pl. 1-3.

INAGAKI, K. (1935) Some marine algae recently

discovered in Japan and new to Science.

Scient. Pap. Inst. algol. Res. Hokkaido Univ.

1(1), 41-49.

Kyiin, H. (1925) The marine red algae in the

vicinity of the Biological Station at Friday

Harbor, Washington. Acta Univ. lund., N.F.

21(9), 1-87 including 47 figs.

Toxipa, J. & INABA, T. (1950) Contributions to the

knowledge of the Pacific species of Antitham-

nion and related Algae. Pacif. Sci. 4, 118-134.

WoLLasTon, E. M. (1968) Morphology and taxo-

nomy of southern Australian genera of

Crouanieae Schmitz (Ceramiaceae, Rhodo-

phyta). Aust. J, Bot. 16, 217-417, pl. 1-10.

WoL.LasTon, E. M. (1972) The genus Platytham-

nion J.Ag. (Ceramiaceae, Rhodophyta) on

the Pacific coast of North America between

Vancouver, British Columbia, and southern

California. Syesis 5, 43-53.

NEMATODE PARASITES OF THE KANGAROO ISLAND WALLABY,

MACROPUS EUGENHT (DESMAREST)

1. SEASONAL AND GEOGRAPHICAL DISTRIBUTION

BY LESLEY R. SMALES & PATRICIA M. MAWSON

Summary

The helminths of Macropus eugenii in Kangaroo I. have been identified at least to genus.

Comparison of genus collected in one four-day period from four areas, differing geographically and

ecologically, show differences in their occurrence.

NEMATODE PARASITES OF THE KANGAROO ISLAND WALLABY,

MACROPUS EUGENI) (DESMAREST)

1, SEASONAL AND GEOGRAPHICAL DISTRIBUTION

hy Lestey R. Smares* & Parricia M. Mawsan*

Summary

Smaces, L, Ro & Mawson, P.M, (1978) Nematode parasites of the Kangaroo Island Wallaby,

Macrepus eugenii (Desmarest), 1, Seasonal and geographical distribution. Trans. R. Soe.

S. Aust. 102(1), 9-15, 28 February, 1978.

The helminths of Macropus eugenti in Kangaroo I. have been idenufied at least to genus.

Comparison of species collected in one four-day period from four areas. differing geographically

and ecologically, show differences in their occurrence,

The incidence of strongyle nematodes in the stomach and of their eggs in the faeces,

checked at 2-monthly intervals over two years, shows séasona! variation both of total numbers

and of the constituent species, and this is linked with climatic conditions suitable for reinfesti-

tion with the worms.

Introduction

A systemutic survey of the helminths of ihe

Kangaroo Island Wallaby Mucropus eugenii

(Desmarest) was undertaken preliminary to

work (Smales (976°) on the life history of the

stomach strongyle, Lablestrongylus engenii

(Johnston & Mawson, 1940,),

The wallaby is one of the sinallest macro-

pods. Tts distribution ts now limited to small

populations on the mainland of south-western

Australia and to some off-shore tslands, the

largest of which is Katguroo Island. The hosts

for this study were taken from Kangaroo

Island, where they are still present in large

numbers,

The climate of Kangaroo Island is the Medi-

ferranean type, with most rain falling in winter.

The mean monthly maximum and minimum

temperatures and monthly rainfall recorded at

Kingscote (April 1972—August 1972) or at

Parndana (September 1972-later) were

obtained from the Adelaide Bureau of

Meteorology (Fig. 1). There appears to have

been little, if any, variation, in the temperature

for each month over these four years, though

there is some variation in rainfall—the Septem-

ber fall being low in 1972. the July fall high

in 1974, The general pattern of winter rain

and summer dryness was maintained through-

out the four year period.

The vegetation of Kangaroo Island varies.

from wet sclerophyll forest to open grassland

with serub, the preferred habitat of the wallaby

being dry sclerophyll forest with dense under-

shrubs, This species appears ta be specialised

for life under conditions of much less rainfall

than would support the rainforest or wet

sclerophyll forest where other wallaby species

are found (Ride 1970).

The wallabies were collected frony one or

more of four farm properties, cach in a dif-

ferent part of the island, and with different

plant associations, At Brookland Park, on the

central plateau, with a rainfall of 831 mm a

year, a mallee form of Lucalyprus remota is

dominant. Around Pioneer Bend, also on the

central plateau, with 559-584 mm of rain a

year, E. obliqta and E. casmophylla are the

dominants, At Cape Cassini on the northern

marginal slopes of the plateau, 559-584 mm of

rain, &. eneorifolia is the dominant, associated

with Melaleuca tncinate. An association of E.

diversifolia and E. rugosa, with E. diversifolia

in different forms of mallee ranging from low

* Department of Zoolozy. University of Adelaide, North Terrace, Adelaide, 5. Aust. 5000.

1 Smates, L. R. (1976) A study of the biology of a nematode Lahiastrongylus eugenti (Johnston & Maw-

son) parasitic in the stomach of the tammar wallaby (Maerapuws cugenii (Desmarest)), Ph.D. Thesis,

University of Adelaide (unpublished ).

10 LESLEY R. SMALES & PATRICIA M, MAWSON

z 100)

‘3

1972 1973

AMJJASONDJFMAMJJASONDJS FMAMJJASONDJ FM

we 1975

Fig. |, Maximum and minimum average temperature and rainfall for 1972-1975, Kangaroo island, From

September 1972 taken at Parndana, previously at Kingscote.

tangled shrubs to trees 7.6 m high, is found

at Nepean Bay in the Nepean Embayment low-

land plain, where there is only 483-508 mm of

rain, The species of undershrubs found with

each plant association vary and are controlled

for the most part by edaphic rather than

climatic factors”.

Stands of virgin bush have been left on each

of the farms and these are often sufficiently

large to provide shelter for the wallabies, which

require the protection of dense undershrubs

through the day, and come out into the farm

paddocks at night to feed. Farming procedures

were similar on all properties except that the

clover fields at Brookland Park and Pioneer

Bend were sprayed in August-October of 1973

and 1974 to control Black Spot disease. Kahba-

tiella sp., with Thibenzole (Merck, Sharp &

Dohme). Before this no spray had been used,

At autopsy of each wallaby the stomach wall

was checked for lesions, and a low 10% (by

volume) sample of the stomach contents taken.

This sample as well as the intestinal tract, liver,

and thorax, were eXamined for helminths,

which were collected and fixed in hot 10%

alcohol or 4% formalin, and later identified

and counted.

Geographical variation

In view of the varying rainfall and vegetation

in different parts of Kangaroo Island, we

sampled and compared the helminth fauna of

animals from different areas at more or less

the same date.

Animals were collected from each of the

four areas described above on four consccutive

nights in April 1975. Autumn was chosen

because the heaviest infestations had previously

been observed during autumn and winter, Up

to 10 wallabies were shot in each area. Each

animal was weighed, sexed, and its age deter-

mined from the tooth eruption pattern.!

No helminths were found in the bile ducts

or liver, The species identified were: from the

thoracic cavity, the nematode Dipetalonema

sp.; from the intestine, the nematodes Globo.

céphaloides trifidospicularis Kung 1948 and

Austrastrongylus thylogale Johnston & Maw-

son 1940, and the cestodes Tripletaenia sp..

and Progremotaenia spp. A & B; from the

stomach, the nematodes Cloacina spp., Labie-

sirongylus eugenii (Johnston & Mawson,

1940a), L. longispicularis Wood 1929, Maecro-

postrongylus pearsoni (Johnston & Mawson,

1940b), Oesophagenastes kartana (Mawson,

* Bauer, F, H. (1959) The regional geography of Kangaroo Island South Australia. Ph.D. Thesis. Aus-

tralian National University (unpublished).

NEMATODRFS OF KANGAROO ISLAND WALLABY it

TABLE |

Welmintts collected from M4, engenii on Kangaroo Island during April 1975

Nepean Buy

Cape Cassini

Pioneer Bend Hrookland Purk

Number af wallabies 10 VW 8 10

Mean Mean Mean Mean

No. No. No. No. Na. Na, No, No.

infected worms infected worms infected worms infected worns

Progamulaenia sp. A 3 2 0 i) 0 n “ v

Progamotaenia sp. B | i] {) 0 4 3.5 5 0

Triplotaenia sp- () 0 2 2 | 1 ih} 0

Cloacina spp. R 105 i) 2351 8 S71.3 i] TOT

L, envenii 4 966 9 R744 ' nodule only u ft)

Lu longispicularis 0 ) 4 82.5 ! 40 3 616.7

R. australis 7 582.9 7 4571 8 S875 1m 2272

M, pearsant 5 98 5 124 7 14 iy Rs

O. kartana 2 1p re eli) 3 463.3 h 36.7

Filarinema sp. 2 5.5 0 0 1 1 3 393

G. trifidospiculariy 5 6 5 OR 3 2 4 a3

Ay thyegale 1 720 WwW T2U 4 720 a 2

Dipetalonema sp. 4 i z I 6 | 10 22

1955), Rugepharvie anstralis (MoGnnig 1926)

and Filarinema sp. The species of Cloacéna

were not considered separately as not all of

them have yet been described: they include ©,

curta Johnston & Mawson, 1938, ©, petrogale

Johnston & Mawson, 1938, ©, clarkae Mawe

yon, 1972, C. semealevae Mawson 1975, and C

kartane Mawson 1975. The numbers of each

species or species group from each locality are

shown in Tuble 1,

Filarinema sp. und Labioytrongylus longi-

spicularis both appear to be accidental infec-

tions as they ogceur much more commonly in

the Grey Kangaroo (Afderopus fullpinesus)

{Desmarest) which grazes on the same pastures

as the Kangaroo Island Wallaby, Other species

which have been found io the Grey Kangaroo

as well as in the wallaby are Macrepostronyy lus

pearson’ (rarely), Glohocephuloides — trifide-

ypleularixs (not common) and Rugopharynx

australiy (very common in both host species),

Oevephagonastes kertana is typically found

if the oesophagus of the host, and is collected

from the stomach only when the infestation is

heavy. ‘The vesopbagus was not examined

regularly, and O. kertana may have been

present in some of the wallabies (hough not

recorded from the stomach.

Examination of the stomach wall showed

thal nodules caused hy third stage L. eugenii

larvae! were prescul in all hosts with adult F.

eugenii in the stomach. It will be noted that

the most striking variations in distribution were

m the cases of L. exgenii, Diperalaneima sp.,

and A. thylegale, The incidence of infection

with Cloacina spp. was high from all four

localities, but possibly the actiul species within

the species group varied,

The territorial behaviour and movement pat-

tems of these wallabies have not been studied

although occasional individuals have been

recorded moying up to 16 km (Andrewartha

& Barker 1969). However, those collected in

the present study were probubly from different.

populations, so the observed differences in hel-

minth distibution between the sites represent

real differences in the infestations on Kangaroo

Tsland,

Each of the sampling sites had diferent vege-

tution and soil types. Rykovskii (1972) sug-

gested a close relationship between these fac-

tors and the viability of larval stages of tricho-

strongyles. Together with the differences in

rainfall they may have been important in deter-

mining the distribution of the helminths.

The low incidence of L. eugenit in hosts

from Pioneer Bend and Brookland Park (noted

ulso in other collections from the same area in

1975) is noteworthy because in 1972 and 1973

this species was plentiful there. As mentioned

ubove, the only difference noted in the collec-

tion areas between these periods was the use

of sprays on the pasture.

Seasonal variation

A survey was made of the total sumbers aud

incidence of the different species of strongyles

in the stomach of the wallaby throughout the

Year. It was hoped to find how the wet Winter

and hot dry summer affected the different

specics.

Male wallabies were taken at. two monthly

intervals from April 1972 to Janwary 1974

from Pioneer Bend and Brookland Park, and

subsequently from these and other areas, Until

September 1972 our sample comprised four

12 LESLEY R. SMALES & PATRICIA M. MAWSON

600

400)

MJ. s. N. J M M. J oS. oN. J

1972 1973

May

Eggs per gram (mean)

Fig. 2. Mean faecal egg counts: 1972 to

January 1974.

fe)

Mean number of nematodes.

Mod SON OM OM J,

1972 1973

Fig. 3. Total worm burdens: May 1972-January

1974. The figure at each two monthly

interval is mean obtained from 4-6 male

wallabies.

Ss. oN J

TABLE 2

Occurrence (% of hosts infected) and relative abun-

dance of nematode species collected from the stomach

lumens of 99 wallabies between 1972 and 1975, Abun-

dance expressed as % of largest total number—

107527 Cloacina spp.

Wallabies Relative

infected abundance

Species % %

Cloacina spp. 98 100

L. eugenii 45 76.2

L. longispicularis 20 1.6

R. australis 84 31

M. pearsoni 34 6.5

O. kartana 43 2.5

Filarinema sp. 4 0.03

animals; subsequently 6 animals were taken.

To compare seasonal differences, only the 64

animals from Pioneer Bend and Brookland

Park were used. To compare relative abun-

dance of the different spp., 99 hosts from all

localities were used.

6546.

4000)

Mean number of nematodes,

de Ss. N.

1972

MM.

1973

Fig. 4. Mean bi-monthly occurrence of three

groups of nematodes, May 1972-January

1974.

At each autopsy a faecal sample was taken

and the eggs per gram counted, using a modi-

fied Whitlock counting chamber. Faecal egg

counts (Fig. 2) show peaks of egg production

in May and November of 1972 and 1973, and

in March and November 1974. These peaks

indicate times when the potential number of

infective larvae on the pasture was high.

The stomach of each wallaby was removed

and the contents sieved through bolting silk

(64 mesh/inch”), diluting the retained solid

material to an appropriate volume (200 or 400

ml), and sampling using Clark et al.’s (1971)

method of enabling calculation of worm totals

to a S.D. of +5 worms. All the nematodes in

each sample were fixed in hot alcohol, cleared

in lactophenol, identified and counted.

Mean total worm burdens were determined

for each bi-monthly sample of wallabies (Fig.

3). Highest figures occurred in May and

November 1972 and May and September 1973,

and lowest in September 1972, January and

November 1973, The unseasonably dry weather

(see Fig. 1) experienced earlier may have been

responsible for the low worm burdens recorded

in September 1972. The variation in worm bur-

dens of individual wallabies sampled at the

same time was often large. The oldest and

youngest wallabies usually had the smallest

number of nematodes. Only two young animals

which had just left the pouch had no stomach

nematodes. The relative abundance of each

species was determined by expressing the total

number (collected from 99 tammars), as a per-

centage of the largest total (Table 2). This is

to distinguish between a nematode species

present in large numbers in a few hosts, and

a species present in small to moderate numbers

NEMATODES OF KANGAROO ISLAND WALLABY 13

Maan number of nematodes.

Ma & S Nh tk M M SOS NR

172 73

Fig. 5. Mean bi-monthly occurrences of two nema-

tode speices, May 1972-January 1974.

o——a =aduils

———-o = larvae

‘

NO dk

MJ. . -t S&S NM

i972 1973

Fig. 6. Mean bi-monthly occurrence of adult and

larval Labiestrongylay eugenii. Only in-

fected animals were used to obtain the

mean.

TABLE 3

Seasonal presence or absence of L. engenii in the

stomach lumens of 64 wallabies

Present Absent Total

May 1972 and 1973 7 3 10

July 1972 and 73 7 x) 10

Sept. 1972 and 73 3 7 10

Nov, 1972 and 73 2 8 10

Jan. 1973 and 74 3 9 12

March 1973 and 74 8 4 12

Total 30 34 64

x" 12.53 where x2 (59%) — 11.07 and

ys (2.5%) => 12.83

in a large number of hosts. Only the more

common species, Rugopharynx — australis,

Muacrepostrongylus pearsoni, Oesophagonastes

kartana, Labiostrongylus eugenii and the group

of Cloacine spp., were considered in greater

detail.

The results of the unalysis of seasonal dif-

ference in abundance of each of these species

ure shown to Figs 5 & 6. The 1972 figures for

Cloacina spp. seem to have been influenced by

the dry conditions in September of that year.

The peak for M. pearsoni in January 1974 was

due to one host with an extremely heavy intes-

tation, In all, the periods of heaviest infestation

occurred during the wet season (Cloacina spp.

carly spring, R. australis late autumn and win-

ter, M. pearsoni early autumn, OQ. kartana

autumn and winter months only, L. eugenii late

autunin and winter).

Statistical analysis of the data for L. engenii

(Tables 3 and 4) gave x values statistically

significant at the 5% level, thus indicating that

L. eugenii has a cycle of incidence dependent

on the seasons. For this analysis counts from

March 1974 were included,

The populations of L. ewgenii from each

host were sorted into adults and larval stages

(Fig. 6). No third stage larvae and minimum

of fourth stage larvae were found in the

stomach lumen between September and

January, Observations on the life cycle of L.

eugenii have shown that third stage larvae are

most likely to be acquired between June and

November of any year. These larvae enter the

stomach wall and remain there for about eight

weeks or longer if development is inhibited?.

It is likely that 3rd stage larvae are being

ingested during this period and invade the

stomach wall. Increasing numbers of these lar

vae would be migrating into the stomach lumen

as 4th stage larvae from February onwards.

Comparisons between individual hosts within

the same sample revealed heterogencous age

structures, therefore the number of hasts

sampled was too small to allow statistical

analysis,

TABLE 4

Seasonal ubundance of infection with L. eugenii in 64

wallabies

Number of Z, eugenii

a b c d= Total

May 1972 and 73 4 ie 2 3° Ao

July 1972 and 73 4 1 0 5 10

Sept. 1972 and 73 9 1 0 0 10

Nov. 1972 and 73 9 u 1 0 Ww

Jan. 1973 and 74 10 a] 2 0 12

March 1973 and 74 6 3 1 2 i2

Total no. wallabies 42 6 6 10 64

xt -= 26,77 where x2 (5%) — 28

u—0-500

b—S00-1000

c— 1000-2000

d—2000

14 LESLEY R. SMALES & PATRICIA M. MAWSON

Incidence of infestation of L. eugenii with

respect to host age was also examined. Those

wallabies collected before March 1974 were

grouped according to age, with 36 1—3 years

old in one group and 22 over three years old

in the other. Wallabies less than one year old

were not considered, as they were never found

to harbour L. eugenii (though other species

might be present), An analysis of the incidence

of infection was scored in terms of presence or

absence of the species partly because of the

small host sample size, and partly because of

the practical difficulties involved in estimating

the number of 3rd stage larvae in the stomach

wall. The results of this analysis indicated that

incidence of infection was independent of host

age. The host sample was too small to analyse

in terms of the age structure of the L. eugenii

populations. Therefore it was not possible to

say whether older wallabies have smaller num-

bers of L. eugenii larvae.

It was found that the times of peak egg pro-

duction as determined by faecal egg counts

appeared to be synchronized with those seasons

most advantageous to the nematodes. The peaks

occurring in May were at the time when

weather conditions for survival of infective lar-

vae were good and, in fact, numbers of infec-

tive larvae present on the herbage at this time

have been found to be high.! The November

peak occurred when conditions might have

been too dry for many larvae to survive. How-

ever, such larvae as did reach infectivity did so

at a time when there would be a large number

of susceptible hosts (joeys just out of the

pouch) grazing the pastures. A build up of

infective larvae, from those overwintering as

well as from recent hatching, would be possible

from late winter through to spring.

The total worm burdens fluctuated both sea-

sonally and from year to year. However, there

was a trend towards lowest worm burdens dur-

ing the dryest periods of the year. A number

of workers (Anderson 1972; Gordon 1958;

Parnell 1963) have found that sheep living in

areas with winter rainfall record highest worm

burdens in the late winter and early spring.

Thus it appears that the uptake of infective

larvae of trichostrongyles by domestic stock as

well as strongyles infesting macropods occurs

during or just after wet periods. The success of

these Australian nematode species is probably

related to this synchronisation of their life

cycles with the season. The present study

showed that the majority of 3rd stage L.

eugenii larvae are ingested during the winter

(older wallabies) and spring (wallabies just

leaving the pouch), These develop in the

stomach wall and escape into the lumen from

February on as fourth stage larvae. They

develop to maturity in the stomach lumen, pro-

ducing eggs from late autumn through the

winter. This long prepatent period of about

7-9 months! is probably important in enabling

the synchronisation of life cycle with changes

in seasons.

Seasonal differences in species composition

of worm burdens were also observed. However,

a detailed analysis of the population structures

of species other than L. eugenii was not under-

taken.

Acknowledgments

Our thanks are due to Mr P. Davis for

helping to collect the wallabies and Dr I.

Beveridge for identifying the cestodes. The

work was done with the aid of a grant from the

Rural Credits Development Fund and a Com-

monwealth Postgraduate Research Award.

References

Anperson, N. (1972) Trichostrongylid infections

of sheep in winter rainfall region, 1. Epizoo-

tiological studies in the western district of

Victoria 1966-67. Aust. J. agric. Res. 23,

1113-1129.

ANDREWARTHA, H, G. & BARKER, S. (1969) Intro-

duction to a study of the ecology of the Kan-

garoo Island Wallaby, Protemnodon eugenii

(Desmarest), within Flinders Chase, Kan-

garoo Island, South Australia. Trans. R. Soc.

S. Aust. 93, 127-132.

Crark, C. J., Tucker, A, M. & Turton, J, A.

(1971) Sampling technique for estimating

round worm burdens of sheep and cattle,

Expl Parasitol. 30, 181-186.

Gorpon, H. McL. (1958) The epidemiology of

helminthosis in sheep in winter rainfall regions

of Australia. 2. Western Australia. Aust, vet.

J. 34, 5-19.

Jonnston, T. H. & Mawson, P. M. (1938)

Strongylate nematodes from Central Austra-

lian kangaroos and wallabies. Trans. R. Soc.

S. Aust. 62, 263-286.

Jounson, T. H. & Mawson, P. M. (1940a) On a

collection of nematodes from Australian mar-

supials. Rec. Aust. Mus. 20, 360-366.

Jounston, T. H. & Mawson, P. M. (1940b)

Nematodes from South Australian marsupials.

Trans. R. Soc. S, Aust. 64, 95-100.

NEMATODES OF KANGAROO ISLAND WALLABY 15

Kuna, C. C. (1948) Some new nematodes from

the Australian Wallaby (Macropus rugogrisea

fruticus) with a note on the synonymy of the

genera Zoniolaimus, Labiostrongylus and Buc-

costrongylus. J. Helminth. 22, 93-108.

Mawson, P. M, (1955) Some parasites of Austra-

lian Vertebrates. Trans. R, Soc. S. Aust. 78,

1-7.

Mawson, P. M. (1972) Three new species of the

genus Cloacina Linstow (Nematoda: Strongy-

lata) from macropod marsupials. Trans. R.

Soc. S. Aust. 96, 109-113.

Mawson, P. M. (1975) Two new species of the

genus Cloacina (Nematoda: Strongylida)

from the tammar, Macropus eugenii. Trans.

R. Soc. §. Aust, 99, 39-42.

Monnic, H. O. (1926) Three new helminths.

Trans. R. Soc, S. Afr. 13, 219-298.

PARNELL, I. W. (1963) Helminthosis in sheep in

Western Australia. Aust. vet. J. 39, 220-226.

Ripe, W. D, L. (1970) “A Guide to the Native

Mammals of Australia.” (Oxford University

Press: Melbourne).

Rykovskil, A. S. (1972) Use of indicator plants

for the helminthological evaluation of hunting

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sii po Prirodnoi Ochagovosti Boloznei i

Obschchim Voprosam Parazitologii Zhivot-

nykh, 14-18 Oct. 1969 Samarkand 6(2)

Tashkent, USSR: Izdatel S/VO “FAN”

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THE AUSTRALIAN FROG CHIROLEPTES DAHLIT BOULENGER: ITS

SYSTEMATIC POSITION, MORPHOLOGY, CHROMOSOMES AND

DISTRIBUTION

BY M. J. TYLER, MARGARET DAVIES & MAX KING

Summary

The external morphology, osteology and karyotype of Chiroleptes dahliit demonstrate that this

species is erroneously referred to the Leptodactylidae and is in reality a hylid related to the

southeastern Australian species, Litoria raniformis.

THE AUSTRALIAN FROG CHIROLEPTES DAHLIT BOULENGER: ITS

SYSTEMATIC POSITION, MORPHOLOGY, CHROMOSOMES AND

DISTRIBUTION

by M. J. Tyver,* MarGaret Davies* & MAX KINGy

Summary

Tyibr, M. J.. Davies, M, & Kona, M. (1978) The Australian frog Ch/rolepres dalilii Boulenger:

its systematic position, morphology, chromosomes and distribution, Trans. R. Sec. 8. Aust.

102(1), 17-23, 28 February, 1978.

The external morphology, osteology and karyotype of Chirelepres dallti demonstrate that

this species is erroneously referred to the Leptodactylidae and is in reality. a hylid related to

the southeastern Australian species, Litorta raniformits.

Introduction

The Australian frog Chiroleptes dahlii

Boulenger (1895) was based on two speci-

mens taken at Daly River, Northern Territory

by Dahl. Despite its comparatively large size

(up to 85 mm snout to vent length) this spe-

cies has been reported only rarely, so that

little is known of tts morphology. and nothing

of its biology and close phylogenetic relation.

ships. In referring it to the genus Cyelorana

Steindachner, H, W. Parker (1940) had secess

to only one specimen: a syntype.

The second published report of the species

appears to be that of Tyler (1969) who iden-

tified as ©. dahfii frogs from Knuckey’s

Lagoon near Darwin, previously reported as

Hyla anrea by Loveridge (1949). The only

additional published record of C. dahlii is one

of its collection at Edward River in Queens-

land by FP, Parker & Tanner (1971).

Through the assistance of Me G. Miles we

have received and maintained in our labora-

tory u senes of C. dahlii from localities near

Darwin. The striking superficial resemblance

of these frogs to Litoria raniformiy (Kefer-

stein), familiar to us from South Australia,

caused us to examine the systematic position

of dahtii,

Material and methods

Data an external morphology reported here

ure derived privcipally from specimens depo-

sited in various museum collections abbre-

viated in the text as follows:

Museum of Comparative Zoology, Harvard

University (MCZ)

Northern Territory Museum, Alice Springs

(NTM)

South Australian Museum, Adelaide (SAM)

Western Australian Muscum, Perth (WAM)

Osteological details of dahlil were obtained

trom a series taken at Beaufort Hill near Dar-

win. Those from L. rani/ormis were from the

southeast of South Australia, These prepara-

tions are housed in the University of Adelaide,

Department of Zoology.

Karyological data were obtained from speci-

mens of daklii from Beaufort Hill and Cannon

Hill, and of L. raniformis from Mil Lel, S.A.,

Renmark, S.A. and fnterlaken, Tasmania,

Mitotic chromosomes were obtained from

intestinal epithelial cells using an air dried

technique described by King & Rofe (1976).

Methods of measurements of external fea-

tures follow those described by Tyler (1968),

whilst skull measurements and descriptive ter-

minology follow the pattern adopted by Davies

(1978).

Systematic position

Parker (1940) referred dahlii to the genus

Cyclorana Steindachner, a genus that Tyler

(1970) and Robinson & Tyler (1973) have

shown to exhibit distinct morphological and

! Department of Zoology. University of Adelaide, North Tce. Adelaide, S.A, S000).

* Department of Genetics. University of Adelaide. Present ‘address: Research School of Biological

Sciences. Australian National University.

18 M. J. TYLER, MARGARET DAVIES & MAX KING

Fig. 1. Enlargement of terminal phalanges of the

third toe of a cleared and alizarin stained

preparation of da/ilii showing biconcave,

disc-like intercalary structure (x 12.5).

Abbreviations: ULT = _ ultimate (ter-

minal) phalanx; pen = _ penultimate

phalanx; I.S. = intercalary structure.

biochemical affinities with Australopapuan

frogs of the family Hylidae. More recently the

concept of Cyclorana has changed, and with

the sole exception of dalilii, is composed now

exclusively of squat-bodied fossorial species

(Tyler 1974; Tyler & Martin 1975, 1977).

Heyer & Liem (1976) omit Cyclorana from

their study of Australopapuan leptodactylids

(as myobatrachids), from which action it must

be concluded that they regard it a member of

the Hylidae.

The presence of intercalary structures is

currently diagnostic of the Hylidae but not of

the Leptodactylidae. Noting the presence of

such structures in the species inermis (Peters)

and alboguttata (Gunther), Straughan (1969)

and Tyler (1974) referred these species from

Cyclorana to the hylid genus Litoria. In the

absence of other characters of significance at

the family level we regard any deviation from

this recognition likely to result in the Hylidae

becoming a heterogeneous assemblage.

Examination of the phalanges of C. dahlii

reveals ossified intercalary structures forming

supernumerary bones (Fig. 1). From the hylid

genus Nyctimystes this species is further dis-

tinguished by its horizontal pupil and absence

of a palpebral reticulum. Accordingly we

transfer the species to Litoria and examine its

specific relationships there.

With the removal of daflii from Cyclorana

the latter genus comprises the following spe-

cies:

Cyclorana australis (Gray)

Cyclorana brevipes (Peters)

Cyclorana cryptotis Tyler & Martin

Cyclorana cultripes Parker

Cyclorana longipes Tyler & Martin

Cyclorana maculosus Tyler & Martin

Cyclorana maini Tyler & Martin

Cyclorana novaehollandiae Steindachner

Cyclorana platycephalus (Gunther)

Cyclorana slevini Loveridge

Cyclorana verrucosus Tyler & Martin

Litoria dahlii (Boulenger)

Chiroleptes dahlii Boulenger, 1896, p. 867.

Phractops dahlii: Nieden, 1923, p. 522.

Cyclorana dahlii: Parker, 1940, p. 17.

Material examined: Northern Territory—

SAM R6448, 15930-34, NTM_ 1836-64,

Beatrice Hill (4); SAM R12338, E. Alligator

River; MCZ 25994—-5, Knuckey’s Lagoon;

Queensland—R9674-6. Strathgordon H.S.;

Western Australia— WAM R34601, King

River, 15 km S of Wyndham.

External Morphology

The head is moderately high and slightly

longer than broad (HL/HW 1.01—1.12), its

length equivalent to slightly more than one-

third of the snout to vent length. The distance

between the eye and the naris is greater than

the internarial span (E—N/IN 1.22-1.39). The

SYSTEMATIC POSITION OF CHIROLEPTES DAHLII 19

Fig. 2. Osteological preparations of: A-C, L. dahlii in dorsal, ventral and lateral view; D-F, L.

raniformis in dorsal, ventral and lateral view. Scale = 5 mm.

20 M. J. TYLER, MARGARET DAVIES & MAX KING

canthus rostralis is straight and scarcely dis-

tinguishable. The eye is moderate, its diameter

equivalent to approximately the eye to naris

distance. The tympanum is large and con-

spicuous, its diameter almost equal to the eye

diameter. The vomerine teeth are on two pro-

minent elevations between and behind the

internal choanae, The tongue is broadly oval.

The fingers are elongate, lack lateral fringes

and the tips are scarcely expanded; in decreas-

ing order of length 3> 4 > 1 > 2. The fingers

are unwebbed.

The hind limbs are relatively short (TL/

S-V_ 0.45-0.51). Toes in decreasing order of

length 4 > 5 = 3 > 2 > 1. Webbing is ex-

tremely extensive, reaching the tips of all digits

and separating all of the metatarsals at least

partly.

The skin on the dorsal surface is smooth,

The throat and chest are smooth and the

abdomen and lower thighs very weakly granu-

lar. There is no tarsal ridge.

In preservative, specimens are predomin-

antly various shades of slate with irregular

darker variegations. A mid-vertabral stripe is

commonly present. The back of the thighs are

dark slate with a broad, longitudinal creamish

stripe or a series of large dots.

In life the animal is similarly a basic slate

colour, but there are suffusions of pale green,

particularly on the dorso-lateral surfaces.

Cranial Osteology

Material examined: two dried preparations

(SAM R6448 and a specimen obtained live

from Beaufort Hill); one alizarin preparation

of an entire animal also obtained live from

Beaufort Hill.

The skull is longer than broad, the slightly

clongated snout having a rounded « terminal

tip in dorsal aspect (Fig. 2). The dorsal sur-

faces of the skull are smooth and unorna-

mented, there is no coossification or exostosis

present, and the skin overlying the skull is

freely moveable. There is no evidence of pre-

nasal or dermal sphenethmoid bones. Similarly

there are no lateral flanges nor occipital crests

present,

The nasals are moderately sized and are

narrowly separated medially. The maxillary

processes of the nasals are sharp and slender

and make bony contact with the posterior pro-

cesses of the pars facialis of the maxillary.

They do not extend to the level of the maxil-

lary.

The sphenethmoid is well ossified, with the

nasals extending anteriorly beyond its anterior

terminus, The frontoparietal fontanelle is large

and ovoid.

The orbital margins of the frontoparietals

are straight and postero-laterally the fronto-

parietals do not overlap the crista parotica.

The squamosals are well developed with the

zygomatic ramus being long, extending 76%

of the distance to the maxilla. The otic ramus

is about half the length of the zygomatic

ramus. It does not extend for the whole width

of the crista parotica, but slightly overlaps the

anterior half.

The pterygoid is moderately developed and

the medial ramus is in bony contact with the

otic capsule. The anterior ramus has an exten-

sive articulation with the maxillary at approxi-

mately mid orbit, whilst the posterior ramus

is poorly ossified and articulates with the ven-

tral arm of the squamosal. The quadratojugal

is well developed and articulates anteriorly

with the maxilla and posteriorly with the ven-

tral arm of the squamosal. The parasphenoid

lacks odontoid structures and stretches an-

teriorly almost to the level of the palatines.

The premaxillaries are narrow, toothed

structures and are narrowly — separated

medially. The alary processes are widely

separated, Initially they rise perpendicularly to

the dentigerous processes of the premaxillaries

and then are inclined posteriorly in a hori-

TABLE 1

Cranial features of Litoria aurea group

skull shape:

nasals:

broader than long

articulate with and overlap the

sphenethmoid which projects

anteriorly between, separating

them medially (exception:

alboguttata)

alary processes well developed, inclined pos-

of premaxillary: teriorly at angle no less than

45°

pars facialis

moderately deep, posterior pro-

of maxillary:

cess articulates with maxillary

process of nasal

robust and well developed

well developed, zygomatic

ramus longer than otic ramus.

Otic ramus overlaps crista paro-

quadratojugal:

squamosal:

tica

palatine processes do not articulate with each

of premaxillary: other

dentigerous short, inclined at an angle of

processes 45° to midline.

of prevomers:

SYSTEMATIC POSITION OF CHIROLEPTES DAHLII 21

SSE ph DE a

Sh OBM an BS AX

Be BE Ai BK aa a

KK OAK AK AR RK 45 XE

AA VR,

—>#*

Fig. 3. A—Chromosomes of L. dahlii ¢ from Cannon Hill, N.T. B—Chromosomes of L. raniformis 3

from Mil Lel, S.A. Note the characteristic satellites on pair 13 in both species.

zontal plane. The height of the alary processes

is almost 1.5 times the height of the denti-

gerous processes. The palatine processes of the

premaxillaries do not articulate with each

other. The premaxillaries articulate laterally

with the pars palatina and pars dentalis of the

maxillary.

The prevomers are narrowly separated

medially. They are large, entire and toothed.

Postero-laterally. the prevomers bear wings

forming the anterior, medial and _ posterior

margins of the choanae. The dentigerous pro-

cesses are small and moderately separated.

They lie perpendicular to the midline and bear

8-10 teeth.

The palatines are narrow slender bones

forming the posterior margins of the choanae

with the distal ends slightly expanded and

lying adjacent to the maxillaries. The palatines

do not appear to have postero-ventral shelves.

The maxillary bears a well developed pars

facialis, the posterior process of which arti-

culates with the maxillary process of the nasal.

The pars palatina is very small, extending

ventromedially to the pars dentalis; the maxil-

lary articulates firmly with the quadratojugal

at the level of the prootic foramen.

Karyotype Morphology

All specimens of L. dahlii and L. raniformis

analysed had a chromosome number of 2n =

26. The karyotypes of these species grade

from large to small and the chromosomes are

metacentric or submetacentric. The centro-

meres were in the, same position in corres-

ponding chromosome pairs in both specimens.

A characteristic pair of satellites is present on

chromosome pair 13 in both forms (Fig. 3).

Phylogenetic Relationships

In its gross external morphology, resem-

blance to Litoria raniformis and other mem-

bers of the Litoria aurea group (sensu Tyler

& Davies in press) is quite striking. It shares

with the members of that group, moderate to

22 M, J. TYLER, MARGARET DAVIES & MAX KING

large size, elongate body form, muscular limbs

of moderate length, unwebbed fingers and

strongly webbed toes. The single external

feature unique to dahlii is the degree of web-

bing of the hind foot, which is particularly

extensive in that species.

Osteologically, the cranial features that sup-

port its association with the Litoria aurea

group are listed in Table 1. See also Fig. 2A-F.

Karyotypically, C. dahlii and L. raniformis

have many features in common, Firstly, C.

dahlii has a chromosome number of 2n = 26,

which is the number most often encountered

in the Australian and New Guinea hylids

(Morescalchi & Ingram 1974; Menzies & Tip-

pett 1976). In contrast, all known Australian

leptodactylid species have 2n = 22 or 2n =

24. A number of 2n = 26 was reported for

Cyclorana alboguttatus by Morescalchi &

Ingram (1974). This finding supports the

recent systematic conclusions of Tyler (1974)

who referred C. alboguttatus to the hylid

genus Litoria.

Our unpublished data on the chromosomes

of 35 species of Litoria indicate that many

species may be grouped together by using

characteristics of their chromosome morpho-

logy. C. dahlii and L. raniformis share the

same karyotypic morphology in terms of cen-

tromere position in each chromosome pair,

Moreover, C. dahlii possesses satellites on

pair 13 which are a characteristic of L. rani-

formis and other members of the L. aurea

group. The possession of this presumably

derived condition suggests a close phylogenetic

relationship between C. dahlii and the L. aurea

group.

Geographic distribution of the Litoria aurea

group

Tyler & Davies (in press) illustrated the

distribution of the L. aurea group which has

representatives in southwestern Australia and

then in a continual arc from the southeast to

the northeast. Litoria dahlii now represents the

northern and northwestern species so com-

pleting a pattern of continuous distribution

composed of largely contiguous populations.

Acknowledgments

We would like to thank Mr Greg Miles of

the Northern Territory Fisheries and Wild-

life Branch for the supply of live specimens

of L. dahliii Mr P. Kempster photographed

the toes of L. dahlii. This study was supported

by an Australian Research Grants Committee

grant to M. J. Tyler.

References

BouLeENGER, G. A. (1896) Description of a new

snake and a new frog from North Australia.

Proc. zool. Soc. Lond. 1895

Davies, M. (1978) Variation in the cranial

osteology of the Australopapuan hylid frog

Litoria infrafrenata. Rec. S. Aust. Mus.

17(22).

HEYER, W. R. & Liem, D. S. (1976) Analysis, of

the intergeneric relationships of the Australian

frog family Myobatrachidae Smithson, Contr.

Zool, (233), 1-29.

Kina, M. & Rorg, R. (1976) Karyotypic variation

in the Australian Gekko Phyllodactylus mar-

moratus (Gray) (Gekkonidae: Reptilia).

Chromosoma 54, 75-87.

Loverince, A. (1949) On some reptiles and

amphibians from the Northern Territory.

Trans. R. Soc, S. Aust. 72, 208-215,

MorescaLcui, A. & INGRAM, G. J. (1974) New

chromosome numbers in Australian Lepto-

dactylidae (Amphibia, Salientia). Experientia

30, 1134-5.

Menzies, J. I. & Tippett, J. (1976) Chromosome

numbers of Papuan hylid frogs and the karo-

type of Litoria infrafrenata (Amphibia,

Anura, Hylidae). J. Herpetol. 10(3), 167-173.

NrebeN, F. (1923) Anura 1. In Apstein, C, (Ed.)

Das Tierreich (46) (de Gruyter: Berlin).

ParKER, F. & TANNER, C. (1971) Some frogs from

Southern Cape York Peninsula. N. Qld Nat.

39(155), 4-8.

Parker, H. W. (1940) The Australasian frogs of

the family Leptodactylidae. Novit. zool.

42(1), 1-106.

Ropinson, R. L. & TyLerR, M. J. (1972) The

catecholamine content of the adrenal glands of

frogs as an index of phylogenetic relationship.

Comp. Gen. Pharmacol. 3(10), 167-170.

STRAUGHAN, I, R. (1969) Hyla inermis (Peters),

a species hitherto erroneously referred to the

leptodactylid genus Cyclorana (Anura,

Hylidae/Leptodactylidae). Zooél. Meded.

43(17), 207-212.

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

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

TyLer, M. J. (1969) A synopsis of the frogs of

the genus Ayla of north-western Australia,

with the description of a new species. Rec. S.

Aust. Mus, 16(1), 1-11.

TyLer, M. J. (1970) Patterns of distribution and

the origins of the Papuan hylid frog fauna.

Search 1(5), 246-247.

SYSTEMATIC POSITION OF CHIROLEPTES DAHLII 23

TyLer, M. J. (1974) The systematic position and Ty ver, M. J. & Martin, A. A. (1975) Australian

geographic distribution of the Australian frog frogs of the Cyclorana australis complex.

Chiroleptes alboguttatus Gunther. Proc. R. Trans. R. Soc. S. Aust. 99(2), 93-99,

Soc. Qld 85(2), 27-32.

TyLer, M. J. & Davies, M. (in press) Species Tyver, M. J. & Martin, A. A, (1977) Taxonomic

groups within the Australopapuan hylid frog studies of some Australian leptodactylid frogs

genus Litoria Tschudi. Aust, J. Zool., suppl.. of the genus Cyclorana Steindachner. Rec. S.

(63).

Aust. Mus. 17(15), 261-276.

STRATIGRAPHY OF THE LOWER WILPENA GROUP (LATE

PRECAMBRIAN), FLINDERS RANGES, SOUTH AUSTRALIA

BY P. §S. PLUMMER

Summary

A revised nomenclature is proposed for the dominantly clastic sequence of sediments comprising

the lower Wilpena Group (late Adelaidean) within the Adelaide fold belt. This sequence, herein

termed the Brachina Subgroup, has sharp, locally disconformable lower and upper boundaries,

between which formations are defined on the basis of mappable lithozones.

STRATIGRAPHY OF THE LOWER WILPENA GROUP (LATE

PRECAMBRIAN), FLINDERS RANGES, SOUTH AUSTRALIA

by P. S. PLUMMER*

Summary

PLumMMeR, P, S. (1978) Stratigraphy of the lower Wilpenu Group (late Precambrian), Flinders

Ranges, South Australia. Trans R. Soc. §. Aust. 102(1), 25-38. 28 February, 1978.

A revised) nomenclature is proposed for the dominantly clastic sequence of sediments

comprising the lower Wilpena Group (late Adelaidean) within the Adelaide fold belt, This

sequence, herein termed the Brachina Subgroup, has sharp, locally disconformable lower and

upper boundaries. between which formations are defined on the basis of mappable lithozones.

The Brachina Subgroup displays an upward coursening sequence which represents a

complete phase of regressive sedimentation, ducing which energy conditions became increasingly

vigorous. As the regression progressed, depositional regimes changed from low energy seuling

(from suspension) in a subtidal environment to high energy traction deposition in deltaic plain,

barner-bar and intertidal mud-, and sand-flat environments. Toward the peak of regression ut

least two islands emerged in the central portion of the basin producing local high energy fluvial

10 Marginal murine condivons,

Introduction

Stratigraphic and sedimentologic studies are

usually undertuken with the ultimate aim of

palacogeographic reconstruction. In tegions of

great thicknesses of sedimentary rocks,

especially Where stritigraphic subdivisions ure

based solely upon lithologic erteria—such as

within the Adelaide fold belt—the form of sub-

division must complement this ultimate aim.

The present stratigraphic nomenclature defin-

ing the late Precambrian Wilpena Group (Dal-

garno & Johnson 1964) was devised for in-the-

ficld differentiation of major lithologic units to

be applied ta 1:250 000 scale mapping (Thom-

son 1964), and as such was based on dominant

lithology using one tvpe section as a reference

-Brachina Creek in the central Flinders

Ranges.

The Wilpena Group is, however, readily

divisible into two coarsening-upward cycles, the

lower cycle having a maximum thickness of

approximately 2200 m whilst the upper cycle

uttains about 4000 m. Detailed stratigraphic

Mmupping undertaken throughout the Flinders

Ranges within the lower Wilpena Group hus

identified five separate and distinct mappable

lithozones. Complex intertonguing between

these lithozones. produced by sedimentary

facies changes, renders the present nomencla-

lure inadequate in differentiating belween

depositional environments and thus necessitates

the formulation of a new and workable nomen-

clature to allow unambiguous. application of

such termmology throughout the basin of

deposition. His herein proposed that the lower

Wilpena Group cycle be designated ‘subgroup’

status, whilst the individual jithozones be of

“formation” status. in nceordance with the Aus-

tralian Code of Stratigraphic Nomenclature

(1973),

Present nomenclature

In its type section within Brachina Creck the

lower Wilpena Group rests conformably upon

the sediments of the Umberatana Group (Coats

1964), although local disconfermity is recorded

from parts of the northern Flinders Ranges.

The lowermost unit, the Nuccaleena FPorma-

tion, has at its base a laminated to well-bedded,

pink to cream dolomite, which weathers a bulf

colour and has a maximum thickness of 10 m.

Overlying this is up to 60 m of purple shale

interbedded with occasional dolomite lenses,

which forms a passage into the overlying

Brachina Formation, In the Mount Lofty

Ranges the dolomite unit becomes fenticular

* Department of Geology, University of Adelaide, North Tce. Adelaide. S. Aust. 5000.

26 P. S. PLUMMER

TABLE 1

Stratigraphic nomenclatures for lower Wilpena Group

Mawson

(1939)

Dalgarno and

Johnson (1964)

ABC Range

Quartzite

ABC Range

Quartzite

Brachina

Formation

"chocolate

shales"

Nuccaleena

Formation

and has been equated with a granule-bearing

sandstone with siltstone and dolomite interbeds

—the Seacliff Sandstone Member of the

Brachina Formation (Thomson 1966).

The Brachina Formation comprises brown

and drab olive green, thinly-bedded siltstones

with shale and thin sandstone interbeds total-

ling approximately 1200 m in the type area. To

the southwest of the type area greyish-red silt-

stones and purple shales replace these siltstones,

whilst to the southeast the dominantly green

Ulupa Siltstone (Mirams 1964) has been

defined. Leeson (1970), when mapping the

Beltana area of the northern Flinders Ranges,

identified three major lithozones within the

Brachina Formation and defined them as mem-

bers (see Table 1). Directly overlying the Nuc-

caleena Formation are purple siltstones which

pass upward into drab olive green micaceous

siltstones—the Moolooloo Siltstone Member—

these being overlain by the massive coarse-

grained purple siltstones with minor quartzitic

bands of the Moorillah Siltstone Member. The

uppermost unit is the Bayley Range Siltstone

Member which consists of drab olive green

siltstones with grey fine-grained quartzitic inter-

beds.

Contormably overlying the Brachina Forma-

tion, and capping the lower Wilpena Group, is

a white flaggy crossbedded quartzite—the ABC

Range Quartzite—which is 120 m thick in the

type section (Brachina Creek). This unit

wedges out in an eastward direction where it

is thought to be replaced by the uppermost

siltstones and thin white fine-grained sand-

stones of the Ulupa Siltstone (Binks 1971).

Leeson

(1970)

Proposed New

Nomenclature

ABC Range

Quartzite

ABC Range

Quartzite

Bayley Range

Siltstone Member

Bayley Range

Formation

Moorillah

Siltstone Member

Moorillah

Formation

Brachina

Formation

Moolooloo

Siltstone Member

Moolooloo

Formation

Brachina Subgroup

Nuccaleena

Formation

Nuccaleena

Formation

Although a disconformity marks the top of this

sequence in the southwestern Flinders Ranges,

elsewhere the dominantly purple shales of the

overlying Bunyeroo Formation rest conform-

ably upon the lower Wilpena Group.

Proposed new nomenclature

The lenticularity of the basal Nuccaleena

dolomite along the basin margins and within

the Mount Lofty Ranges, and the wedging out

of the ABC Range Quartzite in an eastward

direction has led to the wide usage within the

literature of the term Brachina Formation in a

context which spans nearly the entire lower

Wilpena Group sequence. However, the three

lithozones identified by Leeson (1970) within

the Brachina Formation are readily recog-

nizable and mappable, both within this forma-

tion and its lateral equivalent, the Ulupa Silt-

stone, throughout the basin of deposition, Also,

the upper two of these lithozones are laterally

equivalent to the ABC Range Quartzite (Fig.

2). It is therefore proposed that the term

Brachina Subgroup be applied to the complete

sequence of sediments lying above the Umbera-

tana Group and below the Bunyeroo Forma-

tion, whilst each of the five lithozones has its

status raised (Where necessary) to formation

level within this subgroup (Table 1). The term

Ulupa Siltstone thus becomes redundant and

should be abandoned.

Type section

Because of the regional intertonguing of the

component lithozones of the Brachina Sub-

group no single type section can be defined to

characterize the full sequence. Also, the present

LOWER WILPENA GROUP STRATIGRAPHY 27

138°34’

To Wilpena

Blinman

Reference

Section

«(Brachina Gorge

ABC Range (ABC)

Wilpena

* Hawker

Middle Gorge (MDG)

Subsidiary

Section

138°03'

ABC Range Quartzite

Barunga,

Bayley Range Formation ap

Moorillah Formation

Moolooloo Formation

Nuccaleena Formation

Fig. 1. Locality map, showing study area and locations of reference and subsidiary sections for Brachina

Subgroup.

28 P. S. PLUMMER

LATE PRECAMBRIAN

(Lower Wilpena Group)

ABC Range Quartzite

Bayley Range Formation

Moorillah Formation

Moolaoloo Formation

Brachina Subgroup

Nuccaleena Formation

Disconformity

Fig. 2. Rock relation diagram for Brachina Subgroup. Lines of section and localities shown on Fig. 1.

type section (in Brachina Creek) suffers from

structural complications and paucity of out-

crop. These problems, therefore, necessitate the

definition of a new reference section and a

subsidiary section (see Fig. | for localities).

The new reference section for the Brachina

Subgroup remains within the central Flinders

Ranges, being defined 0.75 km north of Bun-

yeroo Gorge in the ABC Range at latitude

31°25’S and between longitudes 138°33°30°E

and 138°35’E. This section, totalling 1500 m,

defines the five component subgroup lithozones

and lies within the western limb of an anticline

with a dip of 50° toward the west. The sub-

sidiary section is located in the southern Flin-

ders Ranges 33 km north of Quorn in Middle

Gorge, at latitude 32°06’S and between longi-

tudes 138°02’E and 138°03’E, and lies within

a synclinal western limb which averages a 75°E

dip. This section totals 1150 m and defines the

four component lithozones south of the region

of intertonguing between the shale-siltstone-

sandstone sequence and the ABC Range Quart-

zite. Both sections are readily accessible, and

both display approximately 85% outcrop.

Umberatana Group—W ilpena Group

Boundary

The boundary between the Umberatana

Group and the Wilpena Group was originally

proposed as occurring at the top of the Elatina

Formation and its equivalents (Dalgarno &

Johnson 1964, after Webb & Horwitz 1959).

It therefore separated a series of pebbly, car-

bonate-bearing arenaceous sediments (upper

Umberatana Group) from a series of fint-

grained clastic deposits (the Brachina Forma-

tion) which has a massive to thinly-bedded

dolomite at its base (the Nuccaleena Forma-

tion). Unfortunately, this dolomite becomes

lenticular along the basin margins, in the

Mount Lofty Ranges and the Olary area. Here,

therefore, the boundary between the Umbera-

tana Group and Wilpena Group is marked by

LOWER WILPENA GROUP STRATIGRAPHY 29

Hallett Cove

Thomson 1966) (After Forbes!)

Purple, greyish-red or green

shales & siltstones, often

with dolomite lenses near base

Pink to cream dolomite

Alligator Gorge ABC Range

Moolooloo

(After Plummer?) (This Paper) ©

Red & grey felspathic sandstone

Massive red-brown siltstone

* . Scattered coarse sand, granules

* 9 (often pink) & pebbles

Fig. 3. The Umberatana Group-Brachina Subgroup boundary, separating massive siltstones and sand-

stones with scattered coarse sand, granules and pebbles from shales and siltstones, often display-

ing a massive basal dolomite. Section locations shown on Fig. 1.

!Forbes, B. G.. from field notes.

“Plummer, P. S. (1974) The stratigraphy. sedimentology and palaeoenyironments of the late

Precambrian Umberatana Group in the Mount Remarkable-Alligator Gorge area, South Aus-

tralia. University of Adelaide, B.Sc. (Hons) thesis, unpublished,

the boundary separating pebbly arenaceous

deposits typical of the Elatina facies from

shaley and silty deposits typical of the Brachina

facies. This lenticularity of the Nuccaleena

dolomite has caused confusion in the Olary

region and the Mount Lofty Ranges where a

pebbly felspathic sandstone—the Seacliff Sand-

stone Member—is said to intertongue with, and

replace the Nuccaleena dolomite, because of

the presence of dolomitic interbeds within the

sandstone. Where the Nuccaleena dolomite is

developed in these regions, however, (e.g.

Hallet Cove—Fig. 3) it distinctly overlies the

carbonate-bearing Seacliff Sandstone Member.

30 P. S. PLUMMER

Thus, by the original definition of the Wilpena

Group, and on lithologic criteria, the lower

boundary of the Wilpena Group (and hence of

the Brachina Subgroup) lies at the top of the

uppermost occurrence of pebbly carbonate-

bearing arenaceous sediments. The Seacliff

Sandstone Member, therefore is redefined here-

in as the uppermost member of the Elatina For-

mation and equivalents within the Umberatana

Group (Fig. 3).

Nuccaleena Formation

The lowermost unit of the Brachina Sup-

group is a thin to lenticular, though persistent

bed of pink to cream dolomite overlain by

purple shales with thin dolomitic interbeds.

This unit was defined by Dalgarno & Johnson

(1964) as the Nuccaleena Formation. Its

basal contact is locally disconformable upon

the underlying Umberatana Group, whilst its

upper boundary is gradational with the over-

lying Moolooloo Formation. Outcrop of this

unit occurs throughout the basin of deposition,

although the basal massive dolomite becomes

lenticular toward the margins of the basin, in

the Mount Lofty Ranges and the Olary region.

Moolooloo Formation

Regional intertonguing of sedimentary facies

occurs within the — shale-siltstone-sandstone

sequence which gradationally follows the Nuc-

caleena Formation. In the central Flinders

Ranges three separate and distinct lithozones

are readily recognizable, and these are overlain

by the ABC Range Quartzite. In the south-

western Flinders Ranges, however, interdigita-

tion between the upper two lithozones and the

overlying quartzite, and their eventual replace-

ment by the quartzite, leaves the basal litho-

zone as the major representative of the

sequence (Fig. 2). This basal lithozone is

defined as the Moolooloo Formation.

Purple to brown and greyish-red shales and

siltstones with minor fine-grained sandstones

dominate this formation in the type area where

it is 630 m thick. Northward the sequence

becomes finer grained, and in the northern

Flinders Ranges is present as _ well-bedded

shales and fine siltstones, red and purple at the

base, but dominantly grey and green. South of

the type area the sequence shows abundant

graded bedding, from greyish-purple siltstone to

purple shale in beds averaging 1—2 cm thick,

between which thin (less than 1 cm) white fine-

grained sandstones often occur as isolated

lenses. In this region the colour change from

purple to green is encountered as one moves

toward the east (Fig. 5).

Moorillah Formation

In the central and northern Flinders Ranges

the incoming of banded red and white medium-

grained crossbedded quartzite and deep purple

intraformational conglomeratic siltstone inter-

beds marks the boundary between the Mooloo-

loo Formation and the overlying dominantly

well-bedded dark-purple to red-purple shale-

siltstone-sandstone sequence, the Moorillah

Formation. Characteristic of this sequence,

which is 460 m thick in the type area, is the

presence of abundant soft-sediment deforma-

tion structures, generally found within massive,

thickly-bedded purple siltstones (Fig. 6a). In

the southeastern Flinders Ranges, however, this

sequence is generally green, although the

coarser grained sediments retain the purple hue

and still display the soft-sediment deforma-

tional structures, thus allowing ready identifica-

tion of the formation.

Bayley Range Formation

Gradationally overlying the Moorillah For-

mation throughout the Flinders Ranges, with

the exception of the southwestern corner, is a

sequence of drab olive-green, wavy-laminated

to thinly-bedded shales and siltstones with

abundant lenses to thin beds of off-white, fine-,

to medium-grained rippled sandstones. In the

type area this lithozone is 300 m thick and

commonly displays small-scale soft-sediment

deformation structures. The term Bayley Range

Formation is used to define this unit. Toward

the southwest this formation thickens to an

estimated 650 m until it interdigitates with the

ABC Range Quartzite (Fig. 2).

ABC Range Quartzite

Dalgarno & Johnson (1964) modified Maw-

son’s (1939) original definition of the ABC

Range Quartzite by restricting it to the massive

quartzite forming the ABC Range. This defini-

tion is herein retained, although expanded to

include the regional interdigitational relation-

ship with the Moorillah and Bayley Range For-

mations for completeness. Throughout its dis-

tribution in the central and northern Flinders

Ranges the ABC Range Quartzite overlies a

sharp, though conformable contact with the

Bayley Range Formation and consists of mas-

sive off-white, medium-grained crossbedded

quartzite cyclically interbedded with green

siltstones and fine-grained sandstones with thin

to lenticular beds of rippled and crossbedded

fine- to medium-grained sandstone. Generally

LOWER WILPENA GROUP STRATIGRAPHY 31

To Middle Gorge

en ERS

Buckaringa =

Wi =ai Gorge ~

<> G

rere ©

S32

RARE

2, OO

*, re:

popes ert

? 9

> >

2, SOoP ie

. »

% s

AES Bunyeroo Fm

ABC Range Qtz

—_— Moolooloo Fm

ee Region of disconformity

—v-~—__ Disconformity

Fig. 4. Extent of the ABC Range Quartzite-Bunyeroo Formation disconformity, and detailed sketch map

of its outcrop at Buckaringa Gorge. Thicknesses of ABC Range Quartzite are given for measured

sections. Localities not given on figure 1 are: WKG—‘Wuarrakimbo Gorge"; PTG—Pettana

Gorge; WNG—Warren Gorge; and RMG—Richman Gap.

32 P. S. PLUMMER

Palaeoenv™t.

ABC Range Qtz

Bayley Range Fm

Colour

g: grey-green Moorillah Fm

PF Pec pueple Moolooloo Fm

ihe Nuccaleena Fm

HRRRIZZ0000

Palaeoenvironment

S: Subtidal

T: Tidal to low intertidal

|: Intertidal

N: Non=marine

Fig. 5. Subdivision of Adelaide fold belt into major structural regions, and palaeoenvironmental varia-

tions of Brachina Subgroup within these regions.

this facies is overlain by a thin (less than 10

m) massive deep purple coarse-grained to

pebbly crossbedded sandstone, with local inter-

beds of microconglomerates and purple shale

and siltstone. This unit caps the Brachina Sub-

group and underlies the purple shales of the

Bunyeroo Formation with a sharp, yet con-

formable contact; isolated lenses of coarse

sand are found within the basal 5 m of the

latter shales. The thickness of the ABC Range

Quartzite in this region ranges from a feather

edge to 80 m.

In the southwestern Flinders Ranges, how-

ever, the ABC Range Quartzite directly over-

lies the Moolooloo Formation. The basal 5 to

100 m of the quartzite in this region comprises

LOWER WILPENA GROUP STRATIGRAPHY 33

Fig. 6, (a) Soft-sediment deformation. Mocrillah Formation. near “Warcowie” Homestead.

(b) Flood-oriented symmetric ripples; flat-topped during ebb tide with late-stage runoff pro-

ducing secondary ripples in troughs (X). Ebb-oriented asymmetric ripples in shallow chan-

nel (Y). Moorillah Formation, ABC Range.

topped ripples (Z). Bayley Range Formation, ABC Range.

(d) Sand waves with superimposed asymmetric ripples. Current from bottom left to top right.

Deltaic plain facies, ABC Range Quartzite, “Warrakimbo Gorge”.

(e) Crossbedding with shale pebbles on foreset faces, and reactivation surface (dashed). Del-

taic plain facies, ABC Range Quartzite, Middle Gorge.

(f) Large polygonal desiccation crack. Deltaic plain facies, ABC Range Quartzite, Woolshed

at.

34 P. S. PLUMMER

massive purple, trough crossbedded, or massive

white to pink, planar crossbedded medium-

grained quartzites, and/or massive deep

purple to grey-green siltstones, all generally

interbedded with purple shales and siltstones.

Following these is the dominant cyclical facies

of the ABC Range Quartzite (now a purple

crossbedded quartzite with purple shale and

siltstone interbeds) which interdigitates with

the Bayley Range Formation. Above this

dominant cyclical facies are deep purple shale-

pebble rich, flat-bedded to shallow crossbedded

siltstones which grade into fine-, and medium-

grained sandstones, overlain by brown to

purple, crossbedded coarse-grained to pebbly

sandstones, which are in turn overlain by mas-

sive white coarse-grained quartzites with gran-

ule beds and occasional microconglomerate

lenses. In this region the ABC Range Quartzite

reaches an estimated maximum thickness of

1800 m (741 m in the subsidiary section) and

appears to conformably underlie, and inter-

tongue with the Bunyeroo Formation—except

in the westernmost segment of this region, west

of longitude 138°02°E, Here pre-Bunyeroo

erosion has scoured deep into the quartzite

leaving a well-defined discontinuity between the

Brachina Subgroup and the Bunyeroo Forma-

tion (Fig. 4).

South of this region, outcropping

sporadically in the Hummock and Barunga

Ranges, is a buff crossbedded sandstone—the

Barunga Sandstone. This sandstone is corre-

lated with the ABC Range Quartzite on the

basis of outcrop pattern, petrologic and palaeo-

current characteristics.

Interpretation of depositional environments

The present configuration of the Adelaide

fold belt appears to reflect the original basin

morphology, at least during Brachina Subgroup

time. Four readily recognizable regions are

present (Fig. 5) displaying differences in their

respective sequences related to variations in

water depth and sediment influx. The temporal

and spatial arrangement of facies within these

sequences, along with their textural and sedi-

mentological characteristics, suggest that the

regional pattern of sedimentation was regres-

sive, with conditions of deposition shallowing

from low energy subtidal, through high energy

tidally dominated deltaic plain, mudflat and

sandflat, to locally high energy fluvial and non-

marine environments.

The two lowermost formations of the sub-

group (viz. the Nuccaleena and Moolooloo

Formations) were deposited under low energy

shallow subtidal conditions. Although initially

clastic deficient, this period of sedimentation

was dominated by the settling of clays from

suspension. Within the central region beds of

silt and fine sand displaying small-scale cross-

lamination, ripple marks and flute casts testify

to the interruption of this quiet environment by

pulses of higher energy traction currents. The

red and purple colouration of these sediments

suggests that conditions of deposition were

oxidizing. In comparison, the Moolooloo For-

mation in the northern and eastern regions

lacks the coarser material and displays a green

colouration, suggestive of greater water depth

(Fig. 7a). The presence of graded beds, groove

casts and rare flute casts—especially in the

eastern region—attest to the existence of trac-

tion currents.

The end of Moolooloo Formation deposition

in the central and northern regions is marked

by pulses of coarser detritus (medium sand

sized) and the shallowing to a low intertidal

mudflat environment, as evidenced by the

presence of tidally oriented ripple mark

associations (Fig. 6b), many being flat-topped.

Thick beds of massive silt displaying abundant

soft-sediment deformation structures (Fig. 6a)

attest to the rapid ingression of sediment into

a saturated environment. The influx of coarser

clastic material—the basal ABC Range Quart-

zite—occurred in the western region. Reactiva-

tion surfaces within sandwave crossbed sets

(Fig. 6d and 6e), flat-topped ripple marks and

large polygonal desiccation cracks (Fig. 6f)

support an intertidal deltaic plain environment

of deposition which is bordered by a barrier-

bar system. Deeper water remained in the

eastern region with green clays and silts still

dominant (Fig. 7b). The Moorillah Formation

is identified in this region by the presence of

red and purple beds of coarse silt and fine sand

which display soft-sediment deformation typical

of the formation elsewhere.

As shallowing through the intertidal zone

gradually progressed and the deltaic plain grew

steadily seaward, the Moorillah Formation was

replaced throughout the basin of deposition by

the green shales and siltstones of the Bayley

Range Formation. Sand interbeds exhibiting

tidally oriented crossbedding and ripple marks,

again often flat-topped (Fig. 6c), along with

the intertonguing of these deposits with those of

the deltaic plain, support the interpretation

of an intertidal mudflat environment for this

formation (Fig. 7c). The green hue of these

LOWER WILPENA GROUP STRATIGRAPHY 35

__ Intertidal

- deltaic plain

Barrier—bar

- Purple

ABC Range Qtz

ubtidal mudflat

Green Moolooloo Fm ——— Intertidal mudflat

—— Bayley Range Fm

Sox Low intertidal mudfiat

“/, Subtidal mudflat

Moorillah Fm

Fig. 7. Palaeogeographic reconstructions through Brachina Subgroup time: A_ subtidal mudflat; B. initial

development of barred delta with adjacent mudflats.

P. S. PLUMMER

Coastal sandflat

_ |, Intertidal

- deltaic plain

ABC Range Qtz * + Intertidal sandflat

ABC Range Qtz

—— Intertidal mudflat

~ _>_ Intertidal mudflat =

Bayley Range Fm Bayley Range Fm

SE Erosion

Palaeogeographic reconstruction through Brachina Subgroup time: C. maximum deltaic pro-

gradation; D. erosion, and development of intertidal sandflat.

LOWER WILPENA GROUP STRATIGRAPHY 37

ONS

| | Tidal mudflat

' Bunyeroo Fm

"| Coastal sandflat

+ (massive)

| | Tidal mudflat

Bunyeroo Fm

‘t*! Non=marine to

varie (ering SANK arans .", Coastal sandflat (massive)

. ABC Range Qtz

ABC Range Qtz

3 Coastal sandflat

—— Intertidal mudflat BR Erosion

Bayley Range Fm

bor Erosion

Palaeogeographic reconstruction through Brachina Subgroup time: E, emergence of islands and

development of associated non-marine deposits; start of transgression; F. transgressive tidal mud-

flat and remnant coastal sandflat.

38 P. S. PLUMMER

sediments, however, is suggested as being due

to greater organic activity® in comparison to the

greens of the underlying formations which

appear to be the result of deposition under

greater depths of water.

The rapid increase in sand content toward

the top of the Bayley Range Formation reflects

continued regression, along with uplift of the

western margin of the basin and the subsequent

erosion of the deltaic plain deposits, forming a

well-defined disconformity in the western

region. Eventually this formation is replaced

by a massive quartzite—the ABC Range

Quartzite—deposited in an intertidal sandflat

environment in the central region with spillover

into the northern and eastern regions (Fig. 7d).

Also, this uplift of the western margin of the

basin caused an influx of coarse- to very coarse-

grained sand from the west which was probably

dispersed along the coast by longshore currents.

Toward the peak of regression the intertidal

sandflat received local injections of coarse

sand of a different provenance. This sand, with

intercalated microconglomerates, forms a

longitudinally oriented cap to the Brachina

Subgroup. The material appears to have been

derived from the regions of the present day

Blinman-Enorama-Oraparinna and Worumba

‘diapir’ complexes and their immediate sur-

rounds in the central Flinders Ranges, and it is

postulated that islands emerged within these

regions shedding the material through high

energy fluviatile and mnon-marine mid-fan

environments into a marine-dominated distal

fan (Fig. 7e).

Despite minor renewed uplift in the western

region and the resultant reworking of sediment

to form a coastal sandflat, a transgression, and

subsequent decrease in sediment influx, pro-

duced very shallow, low energy conditions of

sedimentation under which clays settling from

suspension formed the overlying Bunyeroo For-

mation (Fig. 7f).

Conclusion

Regional stratigraphic mapping has revealed

the presence of five separate and distinct litho-

zones within the lower Wilpena Group that are

persistent and readily recognizable throughout

the Flinders Ranges. Because lithologic criteria

are the basis of subdivision in the late Precam-

brian Adelaidean succession the form of

nomenclature is designed to reflect palaeogeo-

graphic significance. As such, the entire lower

Wilpena Group is herein defined as the

Brachina Subgroup, whilst each individual

lithozone is designated with formation status.

It is the intention behind this nomenclature

that it be applicable to all occurrences of lower

Wilpena Group sediments within the Adelaide

fold belt.

Acknowledgments

For helpful discussion both in the field and

during the preparation of the manuscript the

author extends his thanks to Dr V. A. Gostin.

Valuable criticism concerning the manuscript

was also received from Mr B, Murrell, whilst

Dr B. G. Forbes made available his field notes

of the Olary region.

References

AUSTRALIAN CODE OF STRATIGRAPHIC NOMENCLA-

TURE (1973) J. geol. Soc. Aust. 20(1), 105-

112.

Binks, P. J. (1971) The geology of the ORRO-

ROO 1:250 000 map area, Rep. Invest. Dep.

Mines S. Aust, 36.

Coats, R. P. (1964) Umberatana Group. Quart,

geol. Notes, geol, Surv. S. Aust. 9, 7-12.

Daccarno, C, R. & Jounson, J. E. (1964) Wil-

pena Group, /bid. 12-15.

Leeson, B. (1970) Geology of the Beltana

1:63 360 map area. Rep. Invest. Dep. Mines

S. Aust. 35.

Mawson, D. (1939) The Late Proterozoic sedi-

ments of South Australia. Rep. Aust. N.Z.

Ass, Advmt Sci, 24, 79-88.

Mirams, R. C. (1964 BURRA map sheet, Geologi-

cal Atlas of South Australia, 1:250 000 series,

Geol, Surv. §. Aust., Adelaide.

THomson, B. P. (1964) General outline. Quart.

geol. Notes, geol. Surv. S. Aust. 9, 1-3.

THomson, B. P. (1966) Stratigraphic §relation-

ships between sediments of Marinoan age—

Adelaide region. Ibid. 20, 7-9.

Wess, B. P. & Horwitz, R. (1959) Notes on the

boundaries of the Marinoan Series of the

Adelaide System. Aust. J. Sci. 21, 188-189.

%JIn present day intertidal mudflats where sedimentary structures are well preserved the sediment usually

displays a black colouration due to the reduction activity of abundant microscopic organisms.

CHANGE IN GRAZED ARTIPLEX VESICARIA AND KOCHIA

ASTROTRICHA (CHENOPODIACEAE) POPULATIONS, 1929-1974

BY T. J. FATCHEN

Summary

A vegetation transect laid in virgin Atriplex vesicaria — Kochia astrotricha arid shrubland in 1929

was relocated and sampled in 1974, after 45 years of grazing. The A. vesicaria population was

almost eliminated within the period, and that of K. astrotricha was much reduced. Merits and

difficulties in the re-examination of early data records are highlighted.

CHANGE IN GRAZED ATRIPLEX VESICARIA AND KOCHIA ASTROTRICHA

(CHENOPODIACEAE) POPULATIONS, 1929-1974

by T. J. FATCHEN*

Summary

FATCHEN, T. J, (1978) Change in grazed Atriplex vesicaria and Kochia astrotricha (Cheno-

podiaceae) populations, 1929-1974. Trans. R, Sac. 8. Aust. 102(2), 39-41, 28 February,

1978.

A vegetation transect laid in virgin Atriplex vestcaria — Kochia astrotricha arid shrub-

land in 1929 was relocated and sampled in 1974, after 45 years of grazing. The A. vesicaria

population was almost climinated within the period, and that of K. astrotricha was much

reduced. Merits and difficulties in the re-examination of early data records are highlighted.

Introduction reported, and are still in cxistence at the

The importance of Atriplex and Kochia'

Species to pastoral interests prompted a number

of early investigations into their ecology (e.g.

Cannon, 1921; Murray, 1931). Although most

of the researches were of a descriptive or

anecdotal nature, those of Osborn, Wood &

Paltridge (1932) rehed heavily on quantitative

data, The data records for the 1932 paper in

particular were much more extensive than was

+ Dam

Se Mail road

are Other tracks

——*—Dog fence

Department of Botany, University of Adelaide.

They comprise field notes giving the location

and a general description of the several study

areas: the origin, direction and length of the

transects used in sampling; the number and

position of individuals of target species along

the transects: and the height, widest diameter

and condition of foliage for each individual.

The basic survey technique was the use of belt

\ i Transect ”

\Sandhill 4's Davies Damn’ Fr

\.Dam =’ oo ON /

\ Lyi gers a fi

\ nar fT “Sat oe

- a

\ ~~ a ed Leer \

i ee =--7-™ Billeroo

YES"~_L--4--Bo Hut ~s

ae 2207 i FROME hs

a DOWNS H.S.

Fig. 1. Frome Downs area showing location of transect.

! Nomenclature as in Black's Flora of South Australia.

* National Parks & Wildlife Division, Department for the Environment, Box 1782, G.P.O.,

Adelaide, S. Aust. 5001,

40 T. J. FATCHEN

Table 1: Number of individual plants in transect.

Species Individuals

1929 1974

A. vesicaria 946 4

K. astrotricha 299 80

K. aphylla - 26

K. pyramidata - 9

Total Kochia 299 115

Total shrubs 1245 119

200

150

100

50:

Number of shrubs

1000

2000

Distance (m)

Fig. 2. Distribution of all shrubs in the transect,

1929 and 1974,

transects radiating from stock watering points.

Three were laid in virgin pasture on Frome

Downs station, S. Aust. (Fig. 1), in 1929, each

having a newly sunk dam as its starting point.

These data have received no further attention

since 1932, despite their potential as a baseline

for accurately determining changes in specified

plant populations in the long term. This com-

munication describes the results of re-examin-

ing an early, documented traverse, demonstrates

the standard of information obtainable and

highlights the problems arising on re-examina-

tion.

Methods

Efforts were made to relocate the three

traverses documented by Osborn ef al., but two

of the three could not be found, dams having

either changed their names beyond recognition

or fallen into disuse. The third and longest was

relocated and sampled in March 1974. The

dam at the start of this transect was originally

named Davis’s, but time and changed owner-

ship had corrupted this to Davie’s.

The 1929 scoring methods were followed

(see details in Osborn et al., 1932) with two

exceptions: distance was measured by range-

finder rather than paces, and foliation was not

measured because of the disparity between the

Relative Frequency (°c)

altotala alto

5 & SS + UR 6 Oa a

Og S$ 1 bt Ve 3 Dg” ie US bee

SElt 28 & F HF GE DRM

Diameter Size Class (mm)

Fig. 3. Relative frequency distribution of largest

diameters of K. astrotricha canopies, 1929

and 1974,

1929 and 1974 seasons. The transect was

sampled from the original starting point, but

on a compass bearing allowing for the interven-

ing magnetic variation. All perennial Atriplex

and Kochia species were scored.

The stocking history was sought by reference

to station books, past and present lessees and

the South Australian Pastoral Board.

Results

Stocking history

Stock records for the area are almost non-

existent. Davie’s dam was sunk shortly before

1929, but not stocked because of drought. For

the next ten to fifteen years, sheep may have

watered from it. Cattle certainly watered from

it after 1946, and may have been present from

the start. There are no figures on stocking

variation in the immediate area of the dam.

Rabbits had become established in the area

well before 1929.

Vegetation change

Table 1 summarises the results. The clearest

changes with time are (a) the almost total

POPULATION CHANGE IN ATRIPLEX AND KOCHIA 41

climination of the Atriplex vesicaria population

and (b) the decimation of the Koehia astro-

tricha population, ‘These changes were found

not only in the immediate vicinity of the dam.

but extended throughout the whole transect

(Fig. 2),

K. aphylla, not mentioned at all in 1929,

Was at Significant component of the shrub vege-

tation in 1974. Similarly, some A. pyraniiddta

wus noted in 1974 but not in 1929,

K. astroiricha individuals were smaller in

1974 than in 1929, with the mode of diameter

size class reduced from 31-40 cm to 11-20 cm

(Fig, 3). A proportional change in height was

also noted,

Discussion

Re-exuminution of the transect wnd

evaluation of the resulting data has inherent

difficulties, of Which the worst is determination

of past stocking rates. Although a dramatic

change in the pasture vegetation is documented

here, the cause cannot be indentified with

certainty. Domestic stock grazing is fhe mast

probable, as rabbits were already present in

1929, and no eVidence was found of other

faclors such as fire. Given this. the stecking

levels Which brought about such changes arc

not known, Nor is it certain whether the

changes were gradual or sudden, nor even

which of sheep or cattle initiated the process.

Present experience also indicates that

documentation intended to allow future relo-

cation of study sites must be more thorough

than early investigators realized. No matter

how comprehensive the original field notes,

reference points such as fences or dams can go

oul of commission and memory, or at least

change names with time.

lnsutficiency in the original data may

prevent their most efficient use. For instance,

although Fig. 3 suggests a change in K.

astrotrichd age structures betWeen times, the

original data are not comprehensive enough to

test this adequately: the size structure of a pas-

ture shrub may be largely dependent on season

or grazing pressure. and without supporing

evidence independent of these factors cannot

be tuken as indicative of age structure. As a

further example, both K. apivila and K.

pyramidata may well have increased since

1929; or alternatively may have been of no

interest then and hence not scored,

Nonetheless, despite such limitations, the

repeat of the 1929 observations has. yielded

two significunt results. First, if stocking is the

cause of changes as seems mosi likely, a popu-

lation of K. astrotrieha, albert diminished, can

survive While a much large population of A.

vesicavia is eliminated. Second, irrespective of

Whether sheep or cattle were responsible for

the mitial changes, cattle grazing has at least

maintained the effects of the original impact

since 1946, and may have heen the original

agent. This in turn suygests that the impact

of cattle grazing on these chenopods may not

differ significantly from that of sheep grazing,

Such results far outweigh the attendant

limitations and are relevant im their own right.

Purther examination of the rest of the Oshorn

et ql, data is likely to yield far more extensive

and significant information.

Acknowledgments

The work was funded by the Sandland

Bequest to the University of Adelaide while

the author was recipient of a Commonwealth

Postgraduate Research Award in the Depart-

ment of Botany. Messrs L. D. Wilson and HB. L.

Napier kindly made available facilities on

Frome Downs and assisted in tracing the trans-

ect location.

References

Cannon, W, A. (1921) Plant habitats and habits

in the arid portions of South Australia. Pybl,

Carnesie Iast. (308), 1-139,

Murray, B. J. (19391) A study of the vegetation

of the Lake Torrens Plateau, South Australia.

Trans. R. Soc. 8, Aust. 85, 94-112,

Ossenn. 1. G. B.. Woon, I. G. & PALTRIiDGE, T. B.

(1932) On the growth abd reaction to grazing

of the perennial saltbush Afriplex vesicarinen,

Prec. Linn, Soe. NSW, 37, 377-402.

DEFORMATION HISTORY OF THE OUTALPA AREA AND ITS

APPLICATION TO THE OLARY PROVINCE, SOUTH AUSTRALIA

BY R. F, BERRY, R. B. FLINT AND A. E. GRADY

Summary

The structural and metaphoric history is outlined for a small area of Willyama Complex and its

Adelaidean cover rocks in the central Olary Province. Five penetrative events (three major, two

minor) affect basement rocks, while the final two phases also occur in the cover rocks. The clear

distinction between basement and cover deformations of similar orientation (D3 and Ds) coupled

with a more complete deformation history allows concise interpretation of observable mesoscopic

structures. Four metamorphic events are indicated: a mid amphibolite facies event associated with

the earliest deformation; greenschist facies retrogression associated with the second and third

basement deformations (in basement only), and a final greenschist facies metamorphism associated

with the final two deformation phases. Six significant faults are recognised, three of which post-date

cover deposition. Comparisons made between this area and four others suggest that the general

relations are valid over a wide area of the Olary Province. The structural history determined at

Outalpa is consistent with the history of Willyama Complex rocks at Broken Hill.

DEFORMATION HISTORY OF THE OUTALPA AREA AND ITS APPLICATION

TO THE OLARY PROVINCE, SOUTH AUSTRALIA

by R. F, Berry,’ R. B, FLinr= and A. E. Granv!

Summary

Bemy, Ro F., Puind, R, B. & Grapy, A. B. (1978) Deformation history of the Qulalpa urea

and its application to the Olary Province, South Australia, Trany. R. Soc. S. Ausl (22),

43-53, 2% February, 1978,

The structural and metamorphic history is outlined for a small area of Willyama Complex

und its Adelaideun cover rocks in the central Olary Province. Five penetrative events (three,

major, two Minor) affect basement rocks, while the final two phases also occur in the cover

rocks. The clear distinction between basement and cover deformations of similar orientation

(Dy and Ds) coupled with w more complete deformation history allows concise interpretation

of observable mesoscopic structures, Four metamorphic events are indicaled: a mid amphi-

bolite facies event associated with the eurliest deformation, greenschist facies retrogression

associated with the second and third basement deformations (in basement only), and a final

greenschist facies metamorphism associated with the final two deformation phases. Six signifi-

cant faults fre recognised, three of which post-cate cover deposition. Comparisons mude

between this area and four others suggest thal the general relations are valid over a wide area

of the Olary Province. The structural history determined at Outalpa is consistent with the

history of Willyama Complex rocks at Broken Hill.

Introduction

Crystalline basement tacks of the Olary Pro-

vince form purt of the lower Proterozoic

Willyama Complex which extends from the

Olary region of South Australia fo the Broken

Hill area of New South Wales. At Outalpa

Station, 140 km west of Broken Hill, these

rocks are unconformably overlain by metamor-

phosed upper Precambrian (Adelaidean) sedi-

ments of the Burra and Umberatana Groups.

The broad stratigraphic relationships have heen

established by Campana & King ({958).

The area studied (Figs 1, 4) has a central

granodiorite body that is now fully albitised.

On its castern flank this is partially hounded by

a migmatite zone which grades outwards into

structurally overlying psammitic and pelitic

schists With elongate pods containing corundum

and beryl, Further to the east is a faulted block

of massive, coarse-grained quurtz-leldspar-bio-

ile gneiss.

A high-angle uncontormity separates the

older rocks from the onlapping Adeluidean

sediments. These consist of a lower sequence

of shallow water marine sediments charac-

terised by a discontinuous basal conglomerate,

ond in upper sequence of pebbly siltstones,

shales, quartzites and tillitic units. The lower

and upper sequences are correlated with the

Burra nd Umberatana Groups respectively.

Within the Olary area, the delormational his-

tory of the Willyama Complex and Adeclaidean

metasediments is only poorly known. Talbot

(1967, 1969) has discussed the structural style

at Weckeroo, This report on the Outalpa ayea

gives a more detailed, phase related interpreta-

tion of the deformation history.

Structural interpretation of the Outalpa area

Structural analysis of the area is based on

widespread mesoscopic and macroscopic over-

printing criteria’ and the assumption of

coherence of orientation of tectonic fubric

elements, Fold style could not be used in this

analysis as the different phases can have simi-

lar and overlapping styles which yppear lo be

a function of rock type and deformation inten-

sity.. The history of deformation involves five

‘School of Earth Sciences, Flinders University of S.A., Bedford Park, S. Aust. 5042.

“Geological Survey of South Australia.

R. F. BERRY, R. B. FLINT & A. E. GRADY

140°03

140°05

) Lees

oe 06 “Outalpa Spring

SCALE IN KILOMETRES

Fault __ "=" = Geological boundary

Strike & dip of bedding

Strike & dip of schistosity

LOCALITY MAP

100

KILOMETRES

‘NEW SOUTH WALES

VICTORIA

~~ ADELAIDEAN

LOWER PROTEROZOIC

BURRA UMBERATANA

WILLYAMA COMPLEX

LEGEND

Diamictites, sillstones

& quartzites Bedding trends

as shown

Basal conglomerate

Diorite

Granodiorite

Quartz - biotite gneisses

Sj) trends shown

feldspar

Pelitic schists

Psammitic schists

& quartz granofels

Migmatite zone

$12270 S.A. Dept. of Mines

R.Flint Geologist

Fig. 1. Geological sketch map of the Outalpa Springs area.

DEFORMATION HISTORY OF THE OQUTALPA AREA Af

TABLE |

Supunary of structural and metamorphic events recovnised at Outilpa.

Structural

Camments

Schistosity and gneissosity, Granodtorite intrusion, Mid-

umphibolite facies melamorphismn

Open folding and crenulations

Macroscopic tight folding, strong mesoscopic crenulation

cleavage. Retrogressive zreen-schist facies metamorphism

EROSION

Adeluidean sedimentation; deposition of basal Burra

Group and overlying Umberntana Group sediments

Schistosily in cover metasediments and crenulations in

Basement-cover ifteructions giving tight

syuelines and broad anticlines in the unconformity, Bar-

rovian type Upper greenschist facies Metuamorphism

Cleavage and schistosity in cover metasediments, crenu-

lations in the basement. Open anticline over the gran-

diorite resulling in opposite plunging Fy synclines in cover

rocks, Continuing Barrovian type upper greenschist facies

Event Time Elements

b, Lower Proterozoic Si

Dd: S.Fs

b, Ss.Fy

i, Late Dy faulting

ta Block faulting

UNOONFORM ITY ———

So-ADEL

D, Delamerian Orogeny SuFyty

450-500 m.y. the hasement.

fy Block faulting

D,, S..bs

metamorphism

Late block faulting, producing local horizontal crenula-

tions.

penetrative deformational events anu six fatlts

of which three affect only the basement. This

provides a framework in which to consider in-

formation available from other sections of the

Olary Province, The deformational history is

outlined below and summarised in Table 1,

Deformation | (Dy)

A strong, pervasive Schistosity (S,) defined

by the basal planes of muscovite in the schist

zone and biotite in the granodiorite and mig-

matite zones constitutes the first recognisable

phase of deformation. This schistosity is nor-

mally parallel to remnants of bedding and com-

positional layering, however rare mesoscopic

D, tsoclinal folds were observed, The foliation

i the graiodiorite is parallel to the schistosity

and gneissosity of nearby metasediments.

The granodiovite has an uurcole consisting of

uti inner zone of intense migmatite develop-

ment and an outer zone of feldspar blastesis,

These textures are indicative of temperatures in

the range 650-720°C at 2+ kb (Mchnert

1968), The muscovite content of surrounding

schists decreases (and biotite content increases )

as the more gneigsic and migmatitic terrains are

approached, The gradual disappearance of mus-

covite is expected in the middle amphibolite

facies due Lo the breakdown of its paragonite

component (Thompson 1974) and a range of

reactions with coexisting minerals (Thotmpson

1976). The earliest recognised period of defor.

mation was associyted with amphibolite facies

metamorphism ay has been recorded previously

from other areas of the Willyama Complex

(e.g, Talbot 1967),

Deformation 2 (Ds)

A weak crenulation (Su) is recognised

locally within the Willyama Complex metasedi-

ments. It is restricted to the pelitic units and

has been obscured by later deformational

phases,

Opposite plunging third phase fold axes in

the north of the study area (Fig. 3) suggest

that the second deformation had produced an

open synform in S, prior to both Dy and the

fault t, ‘

Recognition of D. folds is difficult where

no overprinting critena are available, However,

axial planes of crenulations indicate a steep

dip for S,, with @ strike varying from 090°

to 180" but concentrating at 120°, The fold

axes (Fa) have a diffuse orientation, Muscovite

erystallised in the wxial plane of this phase but

the grade of metamorphism could not be deter-

mined, Retrogression of D, mineralogy

probably began during this phase,

Peformation 3 (Ws)

The third phase of folding produced a light

eastward plunging mucroscopie untiform (half

wavelength of 3 km) over the granodrorite

TT So-ADEL

R. F. BERRY, R. B. FLINT & A. E. GRADY

STRUCTURAL ELEMENTS PRE-DATING

ADELAIDEAN SEDIMENTATION

STRUCTURAL ELEMENTS POST-DATING

ADELAIDEAN SEDIMENTATION

ADEL = of ADELAIDEAN

METASEDIMENTS

LP = of LOWER

PROTEROZOIC

METASEDIMENTS

R.Flint Geologist $-12271 S.A. Dept. of Mines

DEFORMATION HISTORY OF THE OUTALPA AREA 47

(Fig. |). The mesoscopic fubrie elements arc

a strong ¢renulation and a crenulation cleavage

in more pelitic rocks. This phase has been mast

effective in redistributing S) and S.,

Third phase axial plane structures (S,) are

constant in orientation (Fig, 2), except tor

slight variations in the southeastern sections

Where fate geierationsy ure strongest (Fig, 3),

Muscovite crystallised in the axial plune af Dy

mesagcepic¢c folds which is compatible with con-

lin\itd telrogressive greenschist facies condi-

tinns.

Adeldidean sedimentation

A major unconformity Lruneates the macro.

scopic De antiform providing a separation of

fold generations into pre- and post-cover.

Adclaideat’ sediments are fault-separated into

an onlapping basal sequence (Burra Group),

and an upper Ulline sequence (Umberatana

Group), Further west, Talbot (1967) has

shown that equivalents of the upper sequence

unconfermahly overtiv the basal sequence:

The Adelaidcan rocks are strongly folded,

The nerthern Outerops of the Burra Group

(Fig. 1. northeast corner) oecupy a tight rorth-

ward plunging syneline, A central pocket of

Nunta Group conglomerates define a small elon-

kote Wusin. Near Outalpa Springs the outcrop

SUpeests a southerly plunging syneline but trans:

position and metamorphism has obscured

bedding ane un exact delineation of the struc.

ture Was fot possible. These three patches ure

not simply celuted as the northern tongue is

associated with a hinge trace which strikes out

weross the hasement west of the southern and

central guteriips. The variation in plunve of the

hinge line of these forth south folds is aseribed

lo the Hlth phase of folding,

Jn the Umberatina Group bedding is strongly

folucd about an east west hinge and the north

trending folds can onty be detected by pertur-

bulls in the eylindrical ature of these

ecusterly trending folds. Note the diffuse nature

of the treat cirele containing poles ta bedding

(S,-AGEL),

Delormation 4 (D,)

The fourth generation of folding tn the

Willyvara Comples metasediments fs eqitiva-

lent to the first event recognised in the cover

rocks. Within the older schists cremulations are

produced wilh NNE striking axial surfaces.

In the basal sequence of the Adeluidean sedi-

ments this phase produced a light syncline with

an axial plane schistosity (S,) defined by bio-

lite, chlorite and actinolite indicating biotite

zone greenschist facies conditians (Winkler

1967). No mesoscopic elements were observed

within sediments of the Umberatana Group.

However, open macroscopic folding of this

upper sequence is inferred from the distribu-

lion of bedding and F,-ADEL (Fig. 2),

The geometry of fourth generation folding

is controlled by the basement cover interaction.

The Gght syncline in the Burra Group is

ussociated with the more schistoye members of

the basement, It is similar in style to the syn-

elines in the unconformity found ai Weekeron

(Talbot 1967). D, mesoscopic structures at

Outalpa predominate in the cover syncline and

ate common in the nearby basement rocks,

They are rare in basement rocks further fram

this contact and were not found! im sedinients

of the Umberatana Group.

The orientation of the |ixial plane of these

Mesoscopic structures (S,) is constant over

most of the area but refracts across the buse-

ment cover contact in the southeastern map

area,

De/erimuation 5 (D.)

The fifth penetrative deformation has pro-

duced casterly trending crenulations and gentle

mycroscopic folds within the Willyama Com-

plex Metasediments. Iv the cover rocks meso-

scopic structural elements vary from a slaty

cleavage in the pebbly silistones and arenites,

to uw schistosity defined by biotite und chlorite

in the pelites. Anticlinal folding of the basal

unconformity has produced a variable plung-

mg complex D, syncline (Fig, 3). Reactivation

of basement structures was restricted to a tight

fold in the southern fault (f;) where §; 4nd

5, are subparallel, and to minor folds in the

conglomerate in the northeastern map urea

where S, and S, are subparallel. No major

tight synclines in the uneonformily were

observed, nor does S, refract across rhe base-

ment-cover boundary (Figs 2, 3),

As 8, and 8S, are steep and strike al 90° to

each other the plunges of F, folds provide an

indication of the geometry of the previously

singly folded Adclaidean bedding. Fold axts

plunges (Fs_auer,) vary over 120° suggesting

Fig. 2. Lower hemisphere equal prea projections of sirvctural data from the Qutalpa area. Contours at

1.2.4.8. 16% per 1% area, Computer contouring using. counting cell area shown in brackets.

Planar vlements plotted as poles.

R. F. BERRY, R. B. FLINT & A. E. GRADY

*‘papnypsul die saxv poy pue sdip sanejuasaiday ‘saodvjins asay} JO ays ay]

UL SUOTRIIBA JURIYIUTZIS SUIMOYS LIRP dIdodsosau PaInsvau! WoOIj 1[Nsai apysodwios ev juasaidal

saury ‘edjeing ie suoneusojap yg ‘Ylp “pig “puz Bulimp psonpord sauvjd [erxe Joj sauly aylg “¢ “SIA

-"¥o eT,

- Dee ,

S3uLIWO1Y

DEFORMATION HISTORY OF THE OUTALPA ARFA 49

Open 10 close fourth generation folds. The con-

centrated maxima for basement fold axes indi-

eates that little reorientation of 5; took place

during the fourth and fifth phases.

Both the cover deformutions (Dy atid D, |

have associated schistosities. S, is restricted to

within the light syneline of the Burra Group.

This was probably the result of un increased

rate of fecovery and reerystallisution due to

higher strain and temperature conditions during

the development of the tight Dy syncline, The

rewionally more significant filth deformation

Was associated with the peak of metamorphic

conditions (upper greenschist facies) for the

cover rocks, Generally, the fifth deformation

had a more homovenous effect an both hase-

ment ail cover tocks. This suggests that feerys-

tallisutian was more advanced and the viscosity

diflerence hetween the two (nits reduced. This

hypothesis is supported by the changing shear

response of the cover. The fault f4, which ts

syn-D, is a shear zone while faults postdaiing

D, (ee) and tS) have a single shear plane,

Faults

Six faults, five of which ate indieuted in

Piz, 1, can be given relative ages from their

interactions with structural elements discussed

previously. They are considered in two groups.

Faults Pre-datiiig Adeldidean Sedimenhition

There are three near-vertical faults whose

movement predates the beginning — of

Adelaidean sedimentation. The Inferred D.,

syntorm (as indicated by the systeniatic change

of Fy plunge) is truncated by the small fault,

f,. The fault is in turn truncated by the uncon.

formity at the base of the Adelaidean sedi-

ments, We conclude that motion on the fault

occurred after D. but before Adeluidean sedi-

mentation. As fF, is subpatalicl ta Sy 4 genetic

relationship js possible. The fault may have

been effected hy the pre-existing S. surface wr

may be an antelinul reverse foull sssocinted

with the D, compression.

The diorite dyke, striking 135° across the

urea (Fig 1), has been injected jnto 9 fault

over the major part of its length. In the central

map area this fault displaces the margin of the

eranodiorite by at least several teus of metres.

Phe fault is locally folded by Dy but the age

relationship of diorite intrusion could pot be

determined.

A large fault, f. hovnds the casiern gneiss

block and is truncated hy ihe unconformity, A

large difference in rock types adjucent to fF.

indicates a large fault movement. Vhe fault ts

unuffected by the third phase deformation and

is the last tecognised phase of tectonic activity

prior to Adelaidean sedimentation,

Faults post-dating Adelaidean Sedimentation

Three faults involve displacement of the

younger metasediments and postdate al least

(hat part of the sedimentation involved in the

units recognised in the study area.

A shear boundary, fs. dipping 80° to the

southeast. beflecis the intense deformation in

the younger metasediments during the fourth

deformation, The intense deformation was

primarily due lo the large variation in com-

pelence between the Willyama Complex meta-

sediments and the Adelaidean melasediments,

Movement continued on fy over @ long period

of time and although it was inifiated prior to

the development of faull 1, ty displaces f,

slightly,

The fault ty is near Vertical with a large

Vertical displacement. Tt ts folded locally by

19, aud is truncated by f>. Movement on f,

was. probably synchronous with the fifth defor-

mutton,

In the southeast a fear vertical fault, ts,

truncates f, and the southern extension of fy.

Within. pelitic racks close to this. fault, a nev

crenulation, dipping at |0° to Q80°, has been

produced, The area af intersection af fy, I, and

I, near Outalpa Springs, is a very complex

crush zone. A simplified interpretation is shawn

in Figure |,

Comparison with other studies

Other structural studies within the Olury Pro-

Vinee have led ip a confused structural history,

This 15 partly due te the large variely of rock

tVpes studied and ibe varying Wetuils estab-

lished. JW an atrempt to synthesise the available

information the probable correlations of stritc-

tures feumt vartaus arcs are hithlighted (Table

2). Areis from Which data afe available are

shown in Figure 4

Hiperaminge Hill

Parker’ and Robertson! discuss in detail a

smiull aren seutheist of Kalabity Homestead.

The carly, pervasive, sillimatite-tmiea schistosity

paralicl to pegmuatitic sexréeations observed

1 Parker, AJ, C1972) A petrological and structural study of « portion of the Olary Province west of

Wiperantinga Hill, S.A. (Unpubl, B.Sc. Hons. Thesis, Univ. of Adel.)

* Roberison, RK. S. (1972) Petrological and structurw! investigation of the Willyuama Complex rocks

Wiperaminga Hill area, S.A. (Unopubl, B.Sc, Hons. Thesis, Univ, of Adel.)

50 R. F. BERRY, R. B. FLINT & A. E. GRADY

TABLE 2

Comparison of structural interpretations from various studies in the Willyama Block (see text for

sources).

OUTALPA WIEERAMINER WEEKERUS MOUNT HOWDEN | BILLEROO HUTS BROKEN HILL

HILL

atlerfalbor

(Irom this paper)

Muscovite biotite

schistosity/gneissosity

D,: Muscovite biotite

schistosity

Muscovite, biotite,

sillimanite schistosity

Sillimanite biotite

schistosity/gneissosity.

Some mesoscopic folds.

Muscovite biotite

schistosity. Mesoscopic

isoclinal folds.

Muscovite biotite

schistosity

Dz: Open macroscopic

folds, Rare

crenulations and

mesoscopic folds

Sillimanite schistosity in

high grade rocks. Weak

open macroscopic folds

insome medium grade

rocks.

Tight upright

macroscopic folds

D,: Tight upright

macroscopic folds.

Common

mesoscopic folds

and crenulations,

Fault f, may be

related to this phase

Tight upright

macroscopic folds

Shear zone

crenulation lage

unknown)

UNCONFORMITY— —

Dy: Tight upright

| macroscopic folds in Basement

the unconformity 7 kinks

Gentle folds in cover

distant from

uncontormity.

Crenulations in the Cover

basement; biotite ‘ schistosity |

muscovite chlorite and cleavage

schistosity in

strongly deformed |

parts of cover °

cover

ee ———

Open crenulations in the

basement. Blotite

| muscovite chlorite

actinolite schistosity in

| Vertical crenulation

cleavage

Subvertical crenulation Open upright

cleavage (possibly a later | macroscopic folds

phase) associated with some of

the retrograde sheer

zones.

Crenulation

(c.f. orientation :

? at Wiperaminga Hill)

Two later sets of Late crenulations

crenulations ?

Ds: Open folds in cover

Gentle folds in the

basement.

Crenulations inthe

basement and

nearby cover. Anew

biotite muscovite

chlorite

schistosity/cleavage

inthe cover, \

chlorite

| Mesoscopic and

macroscopic folds and

crenulations in the cover

A new biotite muscovite

schistosity/cleavage in

parts of the cover,

RE f int Guologes!

correlates well with the S, schistosity of this

study. This schistosity was assumed to be the

axial plane to isoclinal folds. Cross-cutting

relationships of schistosity and bedding were

rarely observed.

Tight macroscopic folds of the early schis-

tosity were developed with an associated biotite-

chlorite schistosity and relatively tight crenu-

lations. These folds have a steeply dipping axial

plane striking from 030° in the west to 105°

in the east, with steeply but variably plunging

fold axes. This phase is correlated with D. at

Outalpa which is also responsible for macro-

scopic folds within the basement.

A weaker late phase is associated with

macroscopic shear zones which dip 80° to 315°.

No apparent correlation exists with the Outalpa

area.

Weekeroo

Talbot (1967, 1969, 1962°) defined several

deformations in the cover and basement north-

78-12 §.A Department ol Mines and Eneigy

west of Weekeroo Station (Fig. 4). Basement

layering and schistosity, defined by muscovite

and biotite, are parallel except in rare isoclinal

hinges. The D, phase (at Outalpa) is corre-

lated with this schistosity.

Within the basement, a crenulation cleavage

with tight macroscopic folds has a subvertical

axial plane striking 070°, with fold axes plung-

ing 60° to 070°, The Dz deformation of our

study is correlated with this folding phase at

Weekeroo,

A later set of kink bands in basement rocks

has moderate to steep axial planes dipping

towards 100°. They may correlate with the S,

phase at Outalpa (dipping 75° towards 090°).

Adelaidean cover metasediments unconform-

ably overlying basement as at Outalpa, are

folded with poles to bedding forming a diffuse

great circle about an axis plunging 40° towards

075°. Axial plane structures developed are a

cleavage in psammites and a schistosity in

* Talbot, J. L. (1962) A study of the structural and metamorphic relationships between older and

younger Precambrian rocks in the Mt Lofty-Olary Arc, South Australia. (Unpubl, Ph.D. Thesis, Univ.

of Adel.)

DEFORMATION HISTORY OF THE OUTALPA AREA 31

“eh Fs ; wa 4

(/BILLEROO HU

iy,

enue Tay

pare a Appt

= he Jreron HS

rai bop BS

ILS,

KILOMETRES,

hla S

yeas!

3S Ay lire ol Meee

Fig. 4, Locality map for areas considered in comparison study. Bedding trend lines shown for cover

mietusediments. Diagram modified from Canipana & King 1958; and Dickson (1975 )*,

pelites. The axial plane predominantly dips. at

80° towards 160°, but the dip direction varies

jiround to 120°, Thisy has been interpreted as a

single phase of deformation,

A bricf study of the mesoscopic structures

by the authors revealed that the basement

crenulation cleavage (Weekeroo) correlated

with S, (Qutalpa) is overprinted by an open

erenulation With an axial plane subvertical and

striking O10", In the cover the earliest schis-

tosity strikes 020° and involves biotite, chlorite

and actinolite as at Outalpa. ft is correlated

with Sy.

This early cover schistosity is folded and

erenulated by a later fold phase which com-

monly has a subvertical axial plane schistosity

striking 040° to 060° which we correlate with

the fifth deformation at Outalpa. A new

cleavage and schistosity is produced in some

areas, This phase at Weekeroo produced tight

short wavelength folds parallel to the third

phase basement structures which Talbot (1969)

has interpreted as basement reactivation

features,

Mount Howden

Flint & Flint? summarised the structure in

the vicinity of the Mt Howden mine. An early

schistosity and gneissosity dre associated with

mesoscopic and macroscopic isoclinal folds. A

later vertical crenulation cleavage, striking

‘Flint, R. B, & Flint, D. J,

(1975) Preliminary geological investigations on the CURNAMONA

1:250000 sheet. S.A. Dept, Mines unpubl. rept. 75/124.

> Nickson, T. W. (1975) Exploration Licence No. 130, Olary Province, 8. Aust. S.A. Dept. Mines Open

File, Env, 2441 (unpubl, )-

52 R. F. BERRY, R. B. FLINT & A. E. GRADY

020°, associated with tight mesoscopic folds is

subparallel to the early schistosity. We corre-

late the schistosity and crenulation cleavage

with the Dy and Ds phases at Outalpa.

At least two later crenulation cleavage phases

were recognised but insufficient evidence was

found to separate them in the area examined.

The axial planes have a variable strike but

always dip steeper than 45° and are probably

equivalent to the later phases at Outalpa.

Billeroo Huts (Flint & Flint)

An early schistosity and gneissosity found in

the Billeroo Huts area is overprinted by a very

strong crenulation cleavage, which is subvertical

and striking 090°. The former surface corre-

lates with S,, but the crenulation cleavage can

not be clearly correlated with Outalpa, It may

be a result of Dz or D5.

A weak late crenulation cleavage with a steep

axial plane striking 050° has no apparent cor-

relation with any structures in our study but is

similar to the shear zone crenulation observed

at Wiperaminga Hill.

Broken Hill

A summary of the structural history of the

Broken Hill area is presented in Glen ef al.

(1977) and a comparison made between struc-

tures of the Gawler and Willyama Domains,

Similar sequence of events and deformational

styles were shown for the two areas.

At Broken Hill in the highest grade rocks,

the first recognised structure is a sillimanite-

biotite schistosity and gneissosity parallel to

layering. This varies to a muscovite schistosity,

which is oblique to layering, in the low grade

rocks. At Outalpa the first deformation has a

schistosity which is subparallel to layering.

The second deformation of Glen er al.

(1977) in the high grade rocks is associated

with a sillimanite-biotite schistosity and tight,

upright folds. However in medium and low

grade areas no mesoscopic structures were

observed and the only suggestion of this defor-

mation is in variations of S, orientation. The

latter case is very similar to D., at Outalpa

where S,, fabrics are rare and variations in S,/

S., intersections have been used to imply a D.

synform.

The third deformation at Broken Hill

developed upright open folds trending north-

easterly in both high and low grade rocks.

Metamorphism is of variable grade and the S,,

axial plane is defined by mica, chlorite and

more rarely sillimanite. Retrograde shear zones

parallel to S. are probably of the same age

(Glen et al, 1977), At Outalpa, the third period

of deformation produced the dominant macro-

scopic folds. D, folds correlate well in style

and orientation to equivalent generation folds

for the Broken Hill area. The fault f; (Fig. 2)

is parallel to S. and has a similar time conno-

tation to the retrograde shear zones noted at

Broken Hill.

Late crenulations at Broken Hill still await

more precise determinations before adequate

correlations with the 4th and 5th deformations

at Outalpa is possible. However the general

history of weak crenulations and shear zones

is similar for the two areas.

Conclusions

Detailed structural analysis for an area at

Outalpa has established a concise interpretation

of observable mesoscopic structures (Table 1).

This has been possible because the basement-

cover contact between the Wiliyama Complex

and upper Precambrian (Adelaidean) cover

rocks is exposed, allowing distinction between

solely basement and cover deformation phases.

This is particularly important as the final cover

deformation (D;) has a similar orientation to

the much earlier third basement deformation

(Dy).

Five penetrative deformations have been

recognised of which three affect solely basement

rocks. The first event (D,) produced a layer-

parallel foliation in the metasediments and a

foliation in the syntectonic granodiorite. Meta-

morphism during this phase reached mid-

amphibolite facies.

The second deformation (D.) was only a

minor folding phase producing macroscopic

open folds and crenulations. Crystallisation of

muscovite within S. indicates possible initial

retrogressive metamorphism.

Macroscopic tight folding and the intense

development of mesoscopic crenulations and

crenulation cleavage resulted from the third

penetrative event (D.,). Third phase axial plane

structures (S.) are relatively constant in orien-

tation and strike at 065° across the map area.

The crystallization of muscovite in the axial

plane of D. mesoscopic folds is compatible

with continued retrogressive greenschist facies

conditions. Block faulting on f, and f,

occurred prior to Adelaidean sedimentation.

Adelaidean sedimentation and deposition of

the basal Burra Group and overlying Umbera-

tana Group sediments postdate the third

deformation. The first cover phase (D,)

resulted in north-south oriented tight synclines

DEFORMATION HISTORY OF THE OUTALPA AREA 53

and broad anticlines in the unconformity.

Crenulations were produced in nearby base-

ment schists and shearing occurred on fault fy.

Metamorphism during D, reached upper green-

schist facies with a biotite-chlorite-actinolite

schistosity In cover rocks.

The final cover phase (D.) has an east-west

striking axial plane which is very constant in

orientation. An open anticline produced in the

unconformity over the granodiorite has

resulted in the opposite plunging F, synclines

in Burra Group sediments. Structural elements

vary from a slaty cleavage in arenites to a schis-

tosity defined by biotite and chlorite in the

pelites. Continued upper greenschist facies meta-

morphism resulted in further retragression of

basement rocks. The fault f, was locally folded

by this final folding phase.

Comparisons made between Outalpa, other

areas of the Olary Province and Broken Hill

Suggest that the structural history outlined for

Outalpa is valid over a wide area of the

Willyama Complex and Adelaidean rocks.

The structural interpretation at Outalpa pro-

vides a framework to correlate structural

elements over a large part of the Olary Pro-

vince (Table 1). The §, schistosity and

gneissosity are widespread over the entire

Willyama Complex, while D. is responsible for

most macroscopic basement folds. The first

deformation in cover rocks (D,), has resulted

in N-S oriented tight synclines and a second

deformation, D;, has redistributed the plunges

of those synclines and also regionally folded all

cover meta-sediments.

Recent work from Broken Hill (Glen er al.

1977) has allowed a much improved correla-

tion between the structural history al Outalpa

and the more detailed studies within New

South Wales. Structures predating the

Adelaidean unconformity are very similar in

the lwo areas.

Acknowledgments

This work was supported and funded by the

South Australian Department of Mines and the

Discipline of Marine Geology and Geophysics,

Flinders University.

References

CAMPANA, B. & Kinc. D. (1958) Regional peology

and mineral resources of the Olary Province.

Geol. Surv. §. Aust. Bull. 34.

Gipsy, R.A. Lancs, W. P., Parker, A, J, & Rut-

LAND, R. W. R. (1977) Tectonic relationships

between the Proterozoic Gawler and Willyama

Orogenic Domains, Australia, J. geol. Sac.

Aust, 24(3), 125-150.

MEHNERT, K. R. (1968) “Migmatites and the

origin of granitic rocks”: (Elsevier, Amster-

dam.)

Tauror, J, L. (1967) Subdivision and structure of

the Precambrian (Willyama Complex and

Adelaide System), Weekeroo, South Australia.

Trans, Ry Soe, 8, Aust, 91, 45-58.

TaLpor, J. L. (1969) The effects of the Palaeozoic

orogeny on the Precambrian shield of South

Australia. Geol. Ass. Canada, Spec. pap. §,

59-66,

THomeson, A. B. (1974) Calculation of musco-

Vite-paragonite-alkali feldspar phase relations.

Cantr. Miner, Petrology, 44, 173-194,

THompson, A. B. (1976) Mineral reactions in

pelitic rocks. Am. J. Sei., 276, 401-454.

WINKLER, H, G. F. (1967) “Petrogenesis of meta-

morphic rocks,” 2nd ed. (Springer-Verlag,

New York.)

A NEW SPECIES OF THYSANOTUS R.BR. (LILIACAE) FROM EYRE

PENINSULA, SOUTH AUSTRALIA

BY N. H. BRITTAN

Summary

A new species of Thysanotus R.Br. (Liliaceae), T. wangariensis N. H. Brittan from near Port

Lincoln, Eyre Peninsula, South Australia is described and illustrated. It shows similarities with T.

dichotomus (Labill.) R. Br. and T. virgatus N. H. Brittan.

A NEW SPECIES OF THYSANOTUS R.BR. (LILIACEAE) FROM EYRE

PENINSULA, SOUTH AUSTRALIA

by N. H, Brirran*

Summary

Brian, N, H. (1978) A new species of 7h\sanerms R.Br, (Liliaceae) from Eyre Peninsula,

South Australia, Trans, R. See, S, Ausr,, 102(2), 55-57, 28 February, 1978.

A new species of Thysanotus R.Br. (Liliacewe), 7’.

wenwariensis N. H. Brittan From

near Port Lincoln, Eyre Peninsula, South Austvalia is described and illustrated. It shows simi-

larities with 7. dichotomus (Labill.) R.Br. and 7. virgatus N. H. Britten.

Vhysanotus wangariensis N, H. Brittan

sp, nov.

(FIG. 1)

Holotypus: Alcock 815, Hundred of Lake

Wangary, section 524, roadside near Wangary

Hotel, 18xi,1965 (AD 966031110), Lsetypus:

(K),

Herba perennis, wbi matura uphylla. Rhi-

zoma parvum, 5-10 mm diametro, radicibus

rigidis, fibrosis, haud tuberosis. Caules plures,

recti, 20-40 (-50) cm alti, ramificatione

monopodiali-pseudodichotoma, teretes, poreis

basi numerosis, superne 4—5, pilis tuberculatis

ferentibus. Folia 5-7 em long basi caulium

noverum prodientia ante florescentiam mar-

cescentia, Umbellae terminales, floribus 1-3,

bracteis 2—5, duobus exterioribus 1.5-2. mm

longis, Jato-deltoideis, Pedicell 8-10 mm

longi, erecti. Segmenta perianthii 11-12.5 mm

langa, exteriora linearia, 3 mm lata, obscure

4-5-nervatu, interior elliptica, fimbriis 3-3.5

ma) longis. Stamina 6, filamentis circa 2.5 mm

longis, antheris poris terminalibus dehiscenti-

bus, antheris tribus exterioribus 3 mm longis,

reclis, contortis, antheris tribus interioribus

6-7 mm longis, curvatis, contortis. Ovarium

sessile, loculis 3, biovulatis. Stylus terminalis,

curvatus, declinatus, 10 mm longus, Capsula

cylindrica, 5-6 x 3-4 mm, Semina nigra, 2 x

1.5 mm, arillo flavo,

Perennial with small (5-10 mm diam.) rhi-

zome with stiff, fibrous, non-tuberous roots,

Stems several per rhizome, erect-spreading,

20-40 foccasionally to 50) cm tall, monopo-

dially-pseudodichotomously branched, terete,

ridges multiple near base, 4—5 in upper parts,

with tuberculate hairs on the ridges. Bracts

2-3 (occasionally 4) at each node, one: sub-

tending the branch, the other |—2 (occasion-

ally 3) very small, on inner side of axil en-

closing buds leading to the production of 2-3

(occasionally 4) branches from some nodes.

Umbels terminal, 1!—3-flowered, bracts 2-5,

outer two |,5-2 mm long, broadly deltoid,

inner bracts narrower, equal to or shorter than

outer bracts. Pedicels 8-10 mm Jong, erect in

flower and fruit, articulated just above the

level of the apices of the outer bracts. Tepals

11-12.5 mm long; outer three linear, 3-4 mm

wide, obscurely 4—S-nerved; inner three ellip-

tic, 4 mm wide, fimbriae 3-3,5 mm _ long.

Stamens 6, tilaments ca 2.5 mm long, anthers

dehiscing by terminal pore; outer three

anthers straight, twisted, 3 mim long; inner

three anthers curved, twisted, 6-7 mm. long.

The anthers are positioned in two groups of

three, the longer three declinate in the same

direction as the style. Ovary sessile, 3-locular,

2 ovules per loculus. Style termimal, curved,

declinate, 10 mm long. Capsule cylindrical,

5-6 x 3-4 mm, Seeds black, 2 x 1.5 mm, with

yellow aril,

Distribulion: Eyre Peninsula—Wangary and a

few other localities to the N.. N.N.B. and

N.W. of Port Lincoln.

Ecology, At the type locality it occurs in rem-

nants of low heath vegetation on a sandy-loam

soil.

Specimens examined: Spechr 2544, Flora and

Fauna Reserve, Hundred of Hincks, cu 85 km N.

* Botuny Department, University of Western Australia, Nedlands, W-A. 6009.

56 N. H. BRITTAN

STATE HERBARIUM OF SOUTH AUSTRALIA

13/11 [hss bdanienty Hott, See S24, Ma LAKE WANGA Ry

— Rood site. A Rty block Z/S beg, GLB. Catcrers Ne ;

Fig. 1. Holotypus Thysanotus wangariensis N. H. Brittan sp. nov., Alcock 815 (AD 966031110) x

0.43; flower from Brittan 69/03 (cult.) x ca 0.8.

A NEW SPECIES OF THYSANOTUS S7

11.x1.1960 (AD 96107089);

Aleoek 1688, Hundred of Wangary, 40 km

W.N.W. of Port) Lincoln, 14.x1.1967 (AD

96807209); Brittan 69/03, neat Wangary Hotel

(type locality), 29,viii,1969 (UWA); Cleland s.n.,

reserve between Tooligie and Mt Verran, 100 km

N.N.E, of Port Lincoln, 9.x1.1960 (AD

97226204),

of Port Lincoln,

Discussion

In South Australia this species may be con-

fused with T, juncifolius (Salisb.) Willis &

Court (1956), the latter however is usually

erect in habit, from a linear, = cylindrical

rhizome, taller, up to 70-80 cm, the stem not

ridged and with the possible exception of a

region near the base, glabrous. The umbels are

3—5-flowered, the floral bracts whitish and

membranous and usually longer than the

Membranous ouler two bracts. T. wengariensis

has a more spreading habit, ca 40 em (occa-

sionally up to 50 cm) tall, from a compact,

+ spherical, rhizome, umbels 1-2 (occasion-

ally 3)-flowered, the inner bracts shorter than,

occasionally equal to, the two outer bracts,

T. wangariensis most closely resembles the

two non-South Australian species 7’. dichoto-

mus (Labill.) R.Br. (1810)—a Western Aus-

tralian endemic—and 7, virgatus N. H. Brit-

tan—a New South Wales endemic, The

former species both produce leaves in the

juvenile state, those in T. wangariensiy being

shorter and usually more erect than those of

T. dichotomus. The lower parts of the stems

in T. wanearlensis are frequently covered in

long hairs, this condition is rarely found in

T, dichoiomus. The flowers differ in the outer

tepals which are broader (3 mm) compared

with 1,5-2 (rarely 3) mm ol those of T.

dichatomus; they are smooth and obscurely

veined on the outer surface in T. wangariensis,

whereas they are distinctly 3-5-veined and

ridged in T. dichotemus, On the stems only a

single bract, which subtends the branch, is

found per node in TJ. dichotomuy; in T. wan-

gariensis, in addition to this bract, 1-2 (ocea-

sionally 3) others subtend buds, which leads

to the production of 2-3 (occasionally 4)

branches per node in this species,

This feature is also found in T. virgatus, to

Which T. wangariensis bears a close resem-

blance in general habit. 7, virgatuy can be

separated on the basis of floral characters,

especially the wide, 3-4 mm, 6-7-nerved,

outer tepals, inner tepals broader, 5-6 mm

wide, with Jonger fimbriae, 4-5 mm, com-

pared with the 4 mm wide inner tepals and

the 3-3.5 mm long fimbriae of T. wangari-

ensts,

Acknowledgments

The author wishes to express his gratitude

to Mr C, R. Alcock, formerly of Port Lincoln,

for providing transport and hospitality during

his visit to Eyre Peninsula to collect material

of the species, to Dr Hj, Eichler, at that time

Keeper of the Herbarium, Adelaide Botanic

Garden, for permission to consult the collec-

tions, to Dr W. R. Barker for checking the

Latin description and to the University of

Western Australia for the provision of a grant

to enable him to visit South Australia.

References

BRITTAN, N. A. (1972) Thysanotus virgatus sp,

nov. (Lilluceas) from Royal National Park,

New South Wales. Conir. NSW. Nat. Herb.,

4(5), 265-266,

Brown, R. (1810) “Prodromus florae Novae

Hollandiae et insula van Diemen” (J. John-

son, London—in facsimile H, RK, Engelmann,

Weinheim 1960),

Wiitis, J. H. & Court, A. B. (1956) Changes

in’ the nomenclature of three Victorian

monocotyledons. Mwuelleria 1(1), 45.

VOL. 102, PARTS 3 & 4

TRANSACTIONS OF THE

ROYAL SOCIETY

31 MAY, 1978

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Robinson, J. F., Robinson, A. C., Watts, C. H. S. & Baverstock, P. R. Notes on

rodents and their ectoparasites collected in Australia in 1974-75

Milton, B. E. & Twidale, C. R. Structure of the paige Basin, soutera Flinders

Ranges, South Australia - > >

Smales, Lesley R. & Mawson, Patricia M. Nematode and other helminth parasites

of the Kangaroo Island Wallaby, Macropus eugenii (Desmarest).

2. Site selection within the stomach - - - - -

Bye, J. A. T., Dillon, P. J., rage ean tal J. C. & Will, G. D. Bathymngiry a Lake

Eyre - -

Tetzlaff, G. & Bye, J. A. T. Water balance of Lake Eyre for the flooded Petiog

January 1974-June 1976 - - - = =

Roberts, J. D. _ Redefinition of the Australian eect) id frog pia e nes

pictus Peters - - - a uj Py

Dulbusty, J. A. Salt transfers between North and South Lake Eyre - - -

Mawson, Patricia M. Macropicola ocydromi n.g., n.sp. (Nematoda: Strongylidae)

from a Western Australian kangaroo - - - = £

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

NOTES ON RODENTS AND MARSUPIALS AND THEIR ECTOPARASITES

COLLECTED IN AUSTRALIA IN 1974-75

BY J. F. ROBINSON, A. C. ROBINSON, C. H. S. WATTS & P. R. BAVERSTOCK

Summary

One monotreme species, twenty species of marsupials and twenty-seven species of rodents were

taken during a collecting trip in eastern, western and northern Australia between October 1974 and

July 1975. Information is provided on localities, dates, sexes and habitat-type of all species.

Extensions of known ranges were recorded for Rattus villosissimus, Zyzomys argurus, Pseudomys

delicatulus and P. gracilicaudatus. Data on the present location of specimens collected, observations

on the reproductive condition of animals noted in the field and the ectoparasites collected are

included. Comments are made on the low population densities of small mammals in Australia and

the low number of species occurring sympatrically.

NOTES ON RODENTS AND MARSUPIALS AND THEIR ECTOPARASITES

COLLECTED IN AUSTRALIA IN 1974-75

by J. F. Rosinson*, A. C. Rosinsony,

C,H. S, Wartst & P. R. BAverstockt

Summary

Rouwinson, J, F,, Roninson, A, C., Warrs, C. H. S. & Baverstock, P. R. (1978) Notes on

rodents and their ectoparasites collected in Australia in 1974-75. Trans. R, Soc, 8S, Aust,

102(3), 59-70, 31 May, 1978.

One monotrenie species, twenty species of marsupials and twenty-seven species of rodents

were taken during a collecting trip in eastern, western and northern Australin between

QOcloher 1974 and July 1975. Information is provided on localities, dates, sexes and

hubitat-lype of all species. Extensions of known ranges were recorded for Rattus villosissimus,

Zyzomys argurus, Pseudamys delicatulus and P. gracilicandatus, Data on the present. location

of specimens collected, observations on the reproductive condition of animals noted in the

field and the ectoparasites collected are included. Comments are made on the low population

densities of small mammals in Australia and the low number of species occurring sym-

patrically.

Introduction

The distribution and habitat preferences of

the small mammal fauna of Australia is still

very poorly known. Important contributions in

this ficld include—Harrison (1961) and Tate

(1952) for Qld, Calaby (1966) and Marlow

(1958) for N.S.W., Wood Jones (1923) and

Finlayson (1961) for south and central Aus-

tralia, Bannister (1969) and Glauert (1933)

for W.A,, and Calaby & Keith (1974), John-

son (1964) und Parker (1973) for the N.T,

In addition Taylor & Horner (1973) provided

information on all Australian species of the

genus Rattiy.

A. C, Robinson and J. F, Robinson made a

collecting trip between October 1974 and July

1975 in eastern, western and northern Aus-

tralia, The aim was to collect us many differ-

ent rodent taxa as possible during the Ome

available, primarily for studies of their Karyo-

types and blood projcins, Trapping localitres

were therefore chosen to maximise the chances

of capturing specific species, and this generally

involved visiting Known occurrences rather

than trapping in new areas. Overall sampling

was therefore not systematic throughout the

areas covered by the survey, but in any one

locality efforts were made to sample the major

recognisable habitats. This resulted in the cap-

ture of a number of small mammals other than

rodents and details of these are included. In

addition the ectoparasites collected from cach

species are recorded,

Companion papers record the results of an

analysis of the Karyotypes (Baverstock et al.

1975, 1976, 1977a,bc), the blood proteins,

the diet (Watts 1977), and the habitat, of most

of the rodents collected. In addition some

rare and little known ectoparasite taxa will be

discussed in more detail in future papers hy

the relevant authorities listed in the Acknow-

ledgments,

Methods

The route followed on the collecting trip

started at Windorah, Queensland, to Cairns,

then north up Cape York Peninsula as far as

Portland Roads, south through — coastal

Qucensland with a visit to Emerald, then

through coustal N.S.W. (with a visit to Mt

Kosciusko), through coastal Victoria (with a

visit to the Grampians) and then lo Adelaide,

* Department for the Environment, Box 667, G.P.O., Adelaide, S. Aust. S001.

7 National Parks & Wildlife Service, Adelaide.

t Institute of Medical & Veterinary Science, Adelaide.

ao 1. PF. ROBINSON FT AL,

Fig. 1. Localities mentioned in the text.

Collecting on the second half of the trip began

in the southwest of W.A,, then north following

the coast to Broome and Derby; a visit to the

King Leopold Ranges then, via Wyndam, to

Darwin, N.T. From Darwin trips were made

east fo Nourlangie Camp on the edge of

Armbem Land 205 km E, and south to the

Reynolds River. Figure | gives the place

names mentioned in the text. Most species

were collected in live traps although some in-

formation is included on road kills. Forty

Sherman folding aluminium traps, forty wire

mesh cage traps 13 cm s 13 cm x 35 cm, and

fen Wire mesh cage traps 30 em x 25 cm x 45

cm were used. As many of these traps as prue-

licable were set at cach locality. Traps were

placed 20 nmi apart in lines of twenty traps,

with Sherman and small cage traps alternating.

The large cage traps were used only when

attempts were made to capture large species,

ie. Lydramys, Mesembriomys ete. The bait

used Was a mixture of peanut paste and rolled

oats. Normally traps were left down for two

nights in any one location, although shorter

and longer periods were employed, depending

on the species of rodent we were attempting

fo catch, Altogether traps were set on 150

nights for a total of approximately %,500 trap

nights.

The nomenclature used follows Ride (1970)

with the exception of the genus Rares which

is that of Taylor & Horner (1973), as mudi-

fied by Baverstock et al. (1975).

Field identifications were checked in Ade»

laide, using karyotypic as well as morpho-

logical characters. This was particularly im-

portant in Rattus where several species are

difficult to identify while alive, but readily

separated on their karyotypes. In the case of

Queensland Melontys we have followed the

unsatisfactory convention that only two species

are involved: that small animals caught in

grassland are M, Jittoralis, and slightly larger

ones caught in closed forest are M. cervinipes.

However, some individuals could not be clas-

sified in this manner and these are simply

listed as Melonzyy sp. The Northern Territory

Melomys have heen included in M. Jittaralis

provisionally on karyotypic evidence.

The bulk of the paper contains a tabulation

of Jocahties where all the various small mam

mals were caught. Many of these animals were

released subsequently at the points of capture.

They are treated species by species and the

following information is recorded: species

name, common name, specific locality, latitude

south and longitude east, number of indivi-

duals caught (males, females, unsexed), date,

specimen registration numbers, notes on habi-

tat, reproductive condition and ectoparasites.

Localities are given as km on a compass bear-

ing from a recognisable town. Latitudes and

longitudes pinpoint the locality more precisely.

Locahties were regarded as separate when they

differed by more than one minute of latitude

or longitude, No year is given following the

date of collection but all dates fall within the

period October 1974 to July 1975, As many

of the rodents ure still alive at the Institute of

Medical & Veterinary Science at the time of

publication, a dual system of specimen num-

bers is introduced. All specimens have been

assigned an J.M.V.S. publication number and

a list of these will be lodged at the South Aus.

tralian. Museum, and periodically updated.

Where specimens have already been placed in

museums, the appropriate museum registration

number is recorded. Museum abbreviations

usedl are: NMV, National Museum of Vic-

toria; QM, Queensland Museum; WAM,

Western Australian Museum; AM, Australian

Museum; SAM, South Australian Museum.

1.M.V.S. publication numbers have no prefix.

Habitat notes follow the vegetution clussifica-

tion of Specht (1970) and Specht er afl.

(1974), to the level of structural formation,

Resulis

MONOTREMATA

PAMity TACHYGLOSSIDAE

L. Techyelogies aculeatuy, Echidna

Localities: Gle Gi) Maslin Ck, Atherton, (7° 15"

M4530" 4, 21 Nov, (ii) 26 km NW Townsville,

°o" 146°36. 1, 9 Dee,

MARSUPIALS AND RODENTS IN AUSTRALIA 61

Notes: One specimen (1) was trapped near 4

creck bank in m@ cultivated paddock; the other (ii)

on beach dunes covered by low open shrubland.

MARSUPTIALIA

FamMiLy MAcroronipat,

2. Thylogale stigmatica, Red-legged Pademelon

Localities: Qld (1) 72 km S Mt Garnett, 18°14°

144°46', 1, 21 Oct., QM 712. (ii) 4 km S Ather-

ton, 17°18 145"29", 1, 2) Oct., QM 702.

Notes; Both roud kill victiras. Skulls only col-

lected. Adjacent to open grassy woodland (i) and

adjacent to closed forest (ii).

3, Onychogalea unguifera, Northern Nail-

tailed Wallaby

Loculity: H.A. Gi) 19 km SW Wyndham, 16°35°

128°14', 1, 27 May,

Notes: A road kill specimen, skull only collected.

Adjacent to open grassy woodland.

4, Lagorchestes conspicillatus, Spectacled

Hare-wallaby

Loculities: Old G) 74 km N Dajarra, 21°10°

139"40', 1, & October, (ii) 15 km S Mareeba,

17°’ (45°26, 19, 21 Oct, QM 710.

Notes: Both roud kills. Parts of the skull of (i)

und the complete skull of (iip were collected.

Adjagent to tall open shrubland (i) and open

grassy woodland (i),

5, Lagerchesios hirsutuy, Wester Hare-

Wallaby

Locality: W.o4. Gi) Bernier Island, 24°56). 113°9'

4, 00 Apr.

Notes: Four specimens were seen while spot-

lighting on foot in hummock grassland. (Robinson

et al, 1976.)

6, Aepyprymnus rufescers, Rufous Rat-

kangaroo

Locality! Qld (i) 35 km § Proserpine, 20°40°

148°95', | wy Lt Dee, OM 708,

Notes: A road kill specimen. A complete speci

men was collected, Adjacent to open prussy Wood-

land.

7, Bettonvia lesueur, Boodic

Locality: W.4. (i) Bernier Island, 24°55" 113°9"

19, 22 Apr,

Notes: Trapped on the edge of the island platform

in low shrubland (Robinson ef al, 1976),

Reproduction; (i) 1 pouch young C-R length 165

cm,

8, Potorous tridactylus, Potoroo

Loculity; Fie. (2) 6 km SW Bemm River, 37/47"

148'54") 1, 20. Peb.

Notes: ‘Trapped in low open foresi/closed heath

habitat.

FAMILY PHALANGERIDAD

9, Trichosurus Vulpecula, Brush-tailed Possum

Localities: Qld (i) 28 km N Atherton, 17°2°

145°26', 3, 21-22 Nov. (ii) 6 km N Atherton,

17°5° 145"29, 1 9, 23 Nov., QM 714.

Notes: Locality (i) Was 4 garden shed, sur

rounded by open grassy woodland, The road kill

specimen (ii) was adjacent to a road-side strip

of closed forest.

FAMILY PRRAMELIDAR

10, soodon ebesulus, Shori-nosed Bandicoot

Locahty: Vie, (1) 40 km SE Melbourne, 38°15’

145°14', 1, 27 Feb.

Notes: Trapped in low open forest.

11. Iseaden macrourus, Brindled Bandicoot

Localities: Qld (i) 112 km SW Mt Garnett,

18° 36° 144°44', 1 od) 21 Nov, (ii) 7 km SW Port-

land Roads, 12"40° 143°23', 1 3 2 Nov., QM 713.

(iii) 25 km S Cooktown, 15°41° 1457135, | dy 7

Nov. (iv) 8 km SW ‘Townsville, 19°20° 146"4", 2,

7 Dec. (v) 26 km NW. Townsville, 19°9'

146°36, 3, 9 Dec. (vi) 58 km N Maryborough,

25°6" 182°32. 19, 14 Jan. N\S.W. (vii) 20 km

SW Port Macquarie, 31°37’ 153°50", 1 1 Feb,

N.T. (viii) 185 km E Darwin, 12°41" 132°55',

18, 15-17 June. (ix) Vicinity of Nourlangie

Camp, 12°50° 132"41°, 12°46" 132°40", 12°53

132738, 12°54 (32°38, 6, 18-19 June,

Notes; Trapped in a variety of habitats—closed

sedvelund (vi), open grassy forest (i), low grassy

woodland Gii, ix), low open grassy woodland

(iv, viii, ix), closed serub (vii) and low open

shrubland on beach dunes (v). A roud kill speci-

men was collected adjacent to open grassy forest

(ii). Reproduction; (vi) (viii) 2 unfurred pouch

young.

Ectoparasites: (i, iii) Yenopsylla vexabilts.

12. Perameles nasuta, Long-nosed Bandicoot

Locality: Qld (i) 9% km NW Bundaberg, 24°31°

141° 28° 2, W-1t Jan.

Notes; Trapped in closed forest.

Reproduction: (i) 2 independent

trapped,

13, P. howsainville, Barred Bandicoot

Locality: Wed. (1) Bernier Island, 24°56" 113°9',

Lo, 2. 5, 21-22 Apr,

Notes; Five individuals were seen at night in Tow

shrubland. Three individualy were captured in

cuve traps (Robinson er al, 1976),

Reproduction: (i) 2. pouch young C-R length 7

ci.

juveniles

FAMILY DASYURIDAE

14. Dayvurus hallucdtus, Little Northern

Native-Cat

62 J, F. ROBINSON ET AL,

Localities: Gld (i) Coen, 13°96' 143°12", 1 9, 28

Oct. (ii) 272 km S Cooktown, 15°11" 145°12°,

1 4 1 Nov, OM 707, N.T. Gil) Nourtanpie

Rock, 230 km BE Darwin, 12°52’ 132°49, 1, [3

June. (lv) 185 km EB Darwin, 12°41" 132°55', 5,

15-17 June, (v) 24 km NE Nourlangie Camp,

12°40" 132°37', 1 of, 18 June. (vi) 14 km § Nonr-

Jange Camp, 12°54° 132°38', 1, 9 June.

Notes: Localities (iv) and (vi) were low grassy

woodland, Gi) and (v) were road kill victims. on

roads through low grassy woodlands. Nourlangie

Rock is an outlying formation of the Arnhem

Land Escarpment and ean best be described as 5

“rock-pile”, The specimen from Coen was caught

in a feed shed and donated by a local resident,

Reproduction; (1) Lactating female.

Fetuparasites: (1) Nenopsvila vexdbilis, Echidae-

placa mtwrenecebit.

15, Daxyurovides byrnei, Byrne’s Pouched-

mouse

Locality: @ld (i) 75 km SEB Boulia, 15°32"

140°7) 1, 17 Ger.

Notes: One animal was seen af night on 4 flood

Plain covered with tussock grassland.

16. Anfechinus stuartti, Brown Antechinus

Localities; Nu. (i) 20 km SW Port Macquarie,

31°37" 152°52", Id, 2 Feb. (ii) 56 km SE Can-

berra, 35°41' 149°32), 1 do 2 9 14 Feb. AM

M10430. (iii) 20 km NE Mallacoota 37°37°

149°S7", 1 9 1, 17 Feb. Pic. (iv) 6 km SW

Berm River, 37"47' (48°94, 1 6. 20 Feb. fv)

40 km SE Melbourne, 38°)5' 145" 14’, 9, 26-27

Feb, (vi) 38 km E Melbourhe, 37°53" 148°225

9, 1.2 Mar, (vii) 12 km SW Apollo Bay, 38°47'

143°32', 12, 3 Mar. (vill) 73 km NE Hnmilton,

37°18" 142°34@', 6, 7 March,

Notes: A, styarti? was captured in a variety of

habitats: closed scrub (1), open forest (ii), wood-

land/closed heath (iii), low open forest/closed

heath, (iv), low open forest (v), tall open forest

(vi, vii), and closed heath (viil). Tt appears to be

associated with o dense understorey regardless of

canopy heighs.

Ectoparastles: (ti) Pywiopsyila ruinhowll nssp.,

Acanthapsylla rothchildl ssp,

17, Antechinus bellus, Pawn Antechinus

Loculities: N.T, (i) Nourlangie Rock, 244) km B

Darwin, 12°52) 132°49', 1, 13 June, (ii) 185 Km

BE Darwin, 12°40 132°55’,, 6 J, 1 9, 15-17 June,

563, 564. (iii) 1 km S Nourlangic Camp, 12°46°

132°4V, 1d, 19 June, (lv) 10 km S Nourlangie

Camp. 12°50" 132°415 1 ¢, 20 June, 479, fv) 12

km S$ Nourlyngie Camp, 12°53’ 132°38', 1 dy

Tk June, SAM M9896, (vi) 14 km 3 Nourlansie

Camp, 12°54" 132°38, | a, 18 June.

Noles: With the exception of Nourlangle Rock all

localities were woodlaid |abitaly. Nourianuie

Kock is an oullyiny rack of the Arnhem Land

escarpment surmounded hy low grassy woodlatd.

18. dntechinus godmani, Godman’s Antechinus

Locality: Glé (i) 39 km S Innisfail, 17°52"

146°4, 1 od. 5 Dec.

Notes: Caught m closed forest,

Reproduction: 1 independent subadult trapped,

Ectoporasites; Acanhepsvila pavida,

19. Antechinus swainsenti, Dusky Antechinus

Localities; N.S. (i) Kosciuska Natl Pk, 46°23’

148°28', 3d, 4, LO-11 Feb, (ii) 54 km SE Can-

berra, 35°39 149°32', L oy I4 Feb, Git) 56 km

SE Canberra, 35°41 (49°32, | oy l4 Feb, Fie.

tiv) 6 km SW Bemm River, 37°47’ 148°54, 1 9,

20 Feb. (v) 38 km EB Melbourne, 37°53’ 145°22",

3, le2 Mar, (vi) 12 km SW Apollo Bay, 38°47"

143°32', 1, 3 Mar. (vit) 73 km NE Humilton,

37°18" 142°38', |, 7 Mar.

Notes: Caught in a varicty of habitats: closed

grassland (i), open forest (iii), low open forest/

closed heath (iv), tall open forest (v, vi) and

closed heath (vii),

Ectopuarusites: (ii) Pygiepsvila heplla, Acanthe-

avila rothsehildi ssp., GV) A. rothschildi ssp,

20, Sminthopsis rufigenis, Red-cheeked

Dunnart

Locality: Ql? (i) 23 km S$ Portland Roads

120°47° 143°18', L gd, 2 Nov., QM 728.

Notes: Caught tn low open forest/grassy wood-

Tnnel-

21, Sevnthopasls crassicaudata, Fat-tailed

Dunnart

Locality; Qld (1) 70 km SE Boulia, 15°28" 140°4°

1d, 7 Oct, 520,

Notes: Catight on a flood plain in an area of

tussock grassland.

RODENTIA

FAMILY MURIDAR

22. Rattus /uscipes fuscipes, Southern Bush-rat

Localities: Wo. (i) 20 km NW Avgusta, 34°4°

115°?, 2 4,1 8, 6 Apr., WAM M15265-M 15267,

(ii) 22 km NE Jurien, 30°8’ 115"8', 3 2&6 &,

12-13 Apr, WAM M1J5268-M15271 425, 426,

427, 429, 522.

Notes: Locality (i) was a low open woodland/

closed heath formation and (ii) a closed heath

formation.

Ectoparasites: (ii)

Nevopsylla vexabilis,

23, Rattus f. assimilis, Souther) Bush-rat

Localities; Qld fi) 38 km E Kingaroy, 26°39"

s2°13', 1 fd 4 9, 16 Jan., 236, 368. N.S. (ii)

11 km NE Nimbin, 28°32’ 153°18', 1 & 1 9 1,

29 Jan., AM M10401-M10403, (ili) 50 kn NE

Neweastle, 32°39" 152°9", | gf 1 9, 3 Feb., AM

M1L0404, M10414, Civ) Kosciusko Nail Pk, 36°23",

(48°28', 69,5 2, 10-11 Feb. (vy) 54 km SE Can-

Mesolaelaps qaustrallensis,

MARSUPIALS AND RODENTS IN AUSTRALIA 43

berra, 37°39 149°32", 2 ¢, 4 9, 14 Feb, AM

M10408-M10413, (vi) 56 km SE Canberra,

8°41" (49°32), 4 @ 14 Feb, AM M10405-

M10407, 383. (vii) 20 km NE Mallacoota, 37°27°

149°57' G& a, 9 2 1H I7 Feb, Pic. (vill) | km

SW Bemm River, 37°46" 148758, 1 3. 20 Feb.

(ix) 3 km SW Bemm River, 37°47", 148°56', 1,

21 Feb. (x) 5S km SW Bemm River, 37°47"

148°S', 4 df, 9 2, 19-20 Feb, 281-285, 296, 388,

(xt) 6 km SW Bemm River, 37°47° 148°54, 1

1 9, 4, 20-21 Feb. (mil) 38 km E Melbourne,

37°53" 145°22', 5 #3 2, 28 Peb—l Man, 292,

344-399. (xiii) 12 kim SW Apollo Bay, 38°47"

143°32, 7 & 6 Y 7, 3 Mar, 211, 293, 246,

400-404.

Notes: Caueht in closed forest ( and ii), open

forest (iil, v amd vi), closed grassland (iv), wood-

land/elosed heath (vi), Jow open forest/closed

healh (Vil), cloged serub (vii) und tall open forest

(vii sand ix),

Reproduction: (i,

juveniles caught,

Fetuparasites: (i, vii, x) Laelaps assimilis, (i, 1,

vi, vii) Laclaps sp.. (vi, vil) Meselaelaps bandi-

coata, (Vil) Gurtheria taylorae, (1, 1V) Maerap-

sya Nerenles, Gv) Pysiopsylla gravis or n.sp.,

(iv, vi, Vii) FP hoplia, (iv, v, vil) P. rainbowit,

(i) Posp, (i) Aeanthepsylla incerta, (vy vi) A

raisehildi ssp. (iv) Stephanacireus econcinntes,

(vii) S. peciinipes.

iv. xii, xiii) Tnelependent

24. Ruitus f, coracius, Southern Bush-rat

Localiues: Old (i) 14 km EB Atherton, 17°15’

148737", 1 &, 2G, 28 Nov, QM 2703, 2121. 347.

fii) 4t km SE Cairns, 17°15° 45°46", 4 J 6 2,

16 Noy,, QM2100, 2706, 2108, 2124, 2126, 354—

357,

Notes: Both loculities were closed forest.

Reproduction: (ii) 3 young born,

Eclopurusites; (i) Pygiopsylla sinuata, Acaithop-

sylla puvida, Slephanectreus dasyuri, Metastiva-

lius rectus, (it) Mesolaelaps australiensis.

25. Rattus lutrealus, Swamp-rat

Loealifes: Old (i) 29 Km B Warwick, 28°16’

52°99, | 2 1, 24 Bel., 367. NSW. Lily 2

km SW Por Macquarie, 21°37° 152°507. 6 ff, 5

9, 1-2 Feb, AM M10422-M 10428, 373-375, 374,

377, 287, 497, 523. 524. Gil) 20 km NE Matha-

eoota, 37°27 149°57", 2 9, 17-18 Feb. AM

M10429_ 376, 377, 387, 497, $23, 524. Vic. (iv)

3 kin SW Hemm River, 37°47" 14856, 4 SL 1

9, 20-21 Beb., 286, 410, (v) G& km SW Berom

River, 97°47, 148"5d Id 4&1, 20-21 Feb..

287, 3K9-391, (vi} 38 km E Sale, 38°6H' 147°31',

19. 33 Feb., 393. (vii) 40 km SE Melbourne,

QRS 145° 14, Foy 264-27 Feb, NMV CiSsesd-

(5688, 405. (wi) 37 km NE Hamilton, 37°35"

142°94', | od. d Mar. (ix) 42 km WE Hamilton,

37°32" 142°25'.2 9. 7 Mar,, 407, 408. (4) 52

km N& Hamilton, 37°27’ 142"28, | 7, 7 Mar,

NMY €15695, (xi) 53 km NE Hamilton, 37°24

142°297, 1 9. 5 Mar., 40% (xii) 73 km NE

Hamilton, 37°18’ 142°36', 2 9, 6-7 Mar, NMV

Cisho4, 294,

Notes: R. latreolus was usually associated willt

damp soil, Habitats were woodland (1), closed

scrub (ii and iv), woodland/closed heath (ii),

closed heath (vi, vii, %, xi, xii). Jow open wood-

land/open heath (vi) and Jow open forest (vil).

Reproduction: (v) 6 young born, independent

juveniles trapped,

Ecloparasites: (ii) Loelaps nutialli, Mesolaelaps

australiensis, (v) M, bandiceata, (ii, ¥) Pygiap-

sila hoplia, (vy P. sp.. Acanthapsylla rothe-

childi ssp.

26. Rattus sordidus, Dusky Field-rat

Localinies: Old (1) 23 km SS Portland Roads,

12°47 143°18', 5 & 4 2 2-3 Nov., QM 2109,

2128, 327, 498-500, 525. (ui) 37 km S Cooktown,

15°48" 145°14, 9 o, 2 Y 8 Nov, 206, 354-337,

Gili) 16 km S$ Cairns, 17°4 145°47. 4d, 2 Ye

14 Nov,, QM 720, 2110-2112, 258, 358. (iv) 17

km S Cairns, 17°5° 145°47°, 2 3 LY, L4 Nov.

(v) 22 Km SE Atherton, 17°22" 145°33°, 2 #4

29 Nov., QM 2102, 253, 348-350. (vi) It km

WE Atherton, 17°12" 45°33. 1) ¢ 9 8, 2, 22

Nov,, QM 2105, 2107, 501-504. (vil} 29 km SE

lnnistail, 17°46 146°7', L, 3 Dee,

Notes: In natural situations KR serdidus was

caught in the following habituts: low open forest/

grassy woodland (i), low grassy woodland [i1),

closed sedgeland (v}, low open grassy woodland

(iv) and open forest (¥ii}. Locality (vl) was a

cane field/closed grassland and Joculity (ii) was

w cultivated paddock/closed grassland.

Reproduction: (ii) Independent juvenile trapped,

Ectoparusites: (i, Di vi) Laelaps nuitalli, (i) £,

sp. (4, ii, iit, vil Mesoluelaps australiensis, (1, \V,

v, Vi) Pygiopsylla heplia, Ge Vv, Va Py rainbow

he sspy (vy. vi) Stephanocirias dasyarl, (Vt) Xenae

pavlla australiaca, A australlacus, (i, ti, vi) X.

verabilis,

27. Rartus collet’, Northern Bush-rar

Loculiliess MF. (4) 175 km E Durwin, 12°42"

132°32. 8 G27 f. 7-8 Jan, SAM M5900, M9902,

4$48-460, i)) 15 ke NE Darwin, 12°33" 130° 56%

a4, 5 9, 11 Tune, SAM M99DI, 461-483, 465,

466.

Notes! Both localities were closed sedgelind.

Rctoparasiles: (i, il) Laelaps nuttalli.

28, Rattus villasissinus, Plague Rat

Loculities: @ld (i) 56 km SE Houlla, 15°22

nu, 2 3 G1 18 Det, 311-313. hii) 72

km SE Boulia, 15°29 140°6, 1, 17 Oct. iii) 77

km SE Boulia, 15°95 40'S, 1 OL 17 Den, 31M,

liv) 32 km W Windorah, 25°20 142718. 5 2

13 Ger, 306-309, (v) 2 km NE ME tsa, 20° aR°

139730, | gd, 39. 19 Get, 314-376. (vi) 33 Em

64 J. F. ROBINSON ET AL,

SE Richmond, 2°49° 143°28", I @, | F, 20 Oet,

3t7, V8 WA, (vii) 26 km SE Wyndham, 15°35"

[28"6"°, 1 gd, 25 May, 441. F

Notes: Cauvehr on gibber plain (i), flood plyins

covered with tussock grassland, (il, Lil, vi, iv),

grassy woodland (v} und closed tussock grass-

land (vii)

Reproduction: (j} Independent juvenile trapped,

Ectoparasires: ti. iit, iv, v, vi) Laelaps paurtallt,

(tv, v) Meselaetaps ausiraliensis, (i, tii, Vv, vi)

Xenopsylla verabilis,

29. Ras |. leucopus, Mottle-tailed Cape

York Kat

Localities: Qld fi) 19 km SW Portland Roads,

12°43’ 143°17". 3 dL 39, 1-3 Nov, OM 2116,

323, 324, 326, 328. (ii) 20 km SW Portland

Roads, [2°44° 143°16', 4 3, 4 2 31 Oct-4 Nov.

QM 729, 2115, 2127, 236, 319-321. (iti) 24 km

SW Portland Rouds, 12°47' 143°18", 1 G31 Oct,

(iv) 26 km SW Portland Roads, 12°44" (43°14,

1d. 3t Oct, (¥) 27 km Portlund Roads, 12°49"

143°18", | dy 1 2 2 Noy.

Notes: All focalities were closed forest.

Reproduction; (li) Female with 5 embryos ip

ulerus, independent juvenile trapped.

Ectoparasites: (i, ii, iii, iv, Vv) Laelaps sp,

30. Rattus leucopus cookrownensis, Motile-

tailed Cape York Rat

Localities: Qld (7) 32 km S Cooktown, 15°45"

145°18', 2 th 4 & &7 Nov, OM 719, 329-332,

339, (fi) 17 km E Atherton, 17°15’ 145°38", 2,

29 Nov.

Notes: Both localities were closed forest.

Ectoparasites: (i) Laelaps sp,

31. Rattus ¢. tuanevi, Tunney’s Rat

Localities: WA, (i) 165 km E Derby, 17°6°

125°10', 1 dy 2 9, 15-16 May, 431-433, (il) 165

km E Derby, 17°7' 125°10', 1 @, 17 May, 436.

(iii) 174 km E Derby, 17°10 125°tH. Id 1 &

18 May, WAM M15303, M1IS5304, (iv) 246 km

E Derby, 17°7', t25°43", 2 & 20 May, 438, $27.

{v) 26 km E Wyndham, 15°35" 128°6, 2 oI 9

25 Muy, WAM M15308, 442, 526, NLT, (vi)

Nourlangie Camp, 12°46' 132°40', 1 oy 1 % 2,

18-19 June, SAM M9912, M9Y9IE. (vii) 1 km &

Nourlungic Camp, 12746" (32°40, 1 3, I) 18-19

June, 471. (vill) 7 Kr SE Nourlaungie Camp,

12°49° 132°42", 3 a. 13 June, SAM M8907, 467,

46%. (ix) & km S Nourlangie Camp, 12°49"

132°40", 1, 19 June. (x) 9 km S Notirlangie

Camp, 12°50" 132°41', | do, 26, 1X-20 June, 529.

(xi) 10 km S Nourlangieé Camp, 12°5t' 132°41',

10, 18-19 Tune. (xii) 14 km S Nourlangie Camp,

12°54" 132°39', 2 dy 9B, 5, 18-19 June, 474-476.

Nutes: Caught in closed tussock grassland (i, ii,

ii, iy. ¥), low woudland/closed tussock grass-

land (lv), low closed forest (vi), low vrassy

woodland (vit, vill, ix, xi, xiii), and low open

grassy woodland (xii),

Eetoparasites: (viii) Lavlaps mertalli, (ali) Afeso-

laelaps australiensis,

32. Rats winneyt culmorum, Tynney'’s Rat

Localities: Qld (i) 22 km SW Emerald, 23°41

148°4" 1d, 15 Dec, 363. (ii) SS km N Rock-

hampton. 22°52" 150°415 1 oY S Jan. QM 2101.

(ii) 58 km N Maryborough, 25°6" 152°33', 14

Tho,, QM 2098.

Notes: Caught im closed grassland (i), low open

forest (i) and grassy woodland (iii),

33. Rattus ratius, Black Rat

Localities: Qld (7) 13 km N Laufa, 15°12"

144°25°, 2 gf, 28 Oct, QM 705, (il) 17 ke S

Caims, 17°5' 145°47', 1G, 14 Nav, 360, (iid

4) km SE Cairns, 17° LS’ 145°546', 2d) LG, 16

Nov,, 351-353, tiv) |! km NE Atherton, 17°12"

(45°39, 1 dy 1 2, 22 Nov, 340-341, tv) Maslin

Creek, Atherton, 17°15) 145°20" - dL oY, 22-22

Nov, 339, 342. (vi) 3 km SE Atherton, (7°20°

45", 1 oy 1G, 27 Nov., 345, 346. {vii) 58

km N Maryborough, 25°6" 152°31' L 9, L4 Jan.

QM 717. {Vib} Mogill Creek, Brishane, 27° 12°

1S2°56' | dg, 1 9, 27 Jan, 369, 370. N.S.W. (ix)

SU km NE Newcastle, 32°39° 152°9', 4 @ 2 9,

3-4 Feb, AM MLO4LS-MLUAIB, 379, (x) 25 km

NW Canberra, 95°O 148°S7' 1 a 1 G9 Feb,

AM MIMI9, MI0420, W.4d_ (xi) 26 km NE

Perth, 31°13" 116°9 Lod, 1 2, 4 April, WAM

M1{S262, 412. (xii) 30 km NW Augusta, 34°4°

ES°2") 1 a 6 May, 4)4, (xt) 18 km N Roe-

fourne, 20°96" 17°10", 2 2 9 May, WAM

M15263, M!5284, N.Y, (xiv) 114 km 8 Darwin,

13°20’ 130°44’, 1 dy 3 2, 24 Tune, SAM M¥903-

M9906.

Noies: Caught in grossy Open forest (i), riverine

closed forest (i), Jow open grussy woodland (ii),

mungroves adjacent to closed forest (iii), closed

grassland (iv), edge of closed forest (vi), open

forest tix), low open forest/closed heath (xii),

rockpile and Whiimmock grassland (xiii) and river

banks fy, a, si. xiv).

Ectopurasites: {ix) Eaelaps assimilis, (iv) Lo muat-

talli (xi) Eehinanyssus bulantanpnsis, Ornlthe-

epssus bacati, (iv) Pygiepsylla ruinbewir t\. ssp,

Oa) FY tenet Ov. ¥) Xenopsylla atstraliaca

(IX, vi) A, Vexabilis, (y, xi) Lepiopsylli segely.

34, Hydromys chrysovasier, Water Rat

Localities; Gi? (i) 63 km NW Cowen, 13°26"

(42°56, | d, 29 Oct. OM #698, (i) 20 km SW

Portland Ronds, 12°44° 143°16°, 2 9 31 Oct-2

Nov. (ili) 26 km S Portland Roads, 12°49"

143°IR, § 3, 2 Nov, tiv) 40 km SE Cairns,

17°15’ 45°56, 2 9 IS Nov, QOM697, iv)

Atherton, 17°15" 145°29" 4 gd 1 9. 24 Nov, 343,

344, OM 699. (Vi) 29 km SE Innisfail, 17°46"

MARSUPIALS AND RODENTS IN AUSTRALIA 65

146°7', 2 ¢, 2 9,4 Dec., 192, 193, 362. (vii) 61

km N Rockhampton, 22°51 80°40" 1 ¢f, 5 Jan.,

365, (vii) 9 km SE Dunwich, Stradbroke Istand..

27°32) 153°30', 1 oy 19 San, 194, WA. (ix) 26

km NE Perth, 31°13 116°91, 2 4,1 9, 4 Apr,

218, 219, 413, (x) 165 km E Derby, t oy i 2

16-17 May, ZLS. 220,

Notes: All localities were at the water's edge:

flowing fresh waler (ii, iii, iv. v, vil, vill, ix, x),

stagnant (4) and saline (vi}-

EBetoparasites: (ill, Vi) Laelaps wasselli, (V) Mexo-

laclaps austruliensis, Pyglapsylla heplia, Neno-

psylla vexuhilin.

35, Mesembriomys gouldli, Black-footed Tree-

rat

Loculities; Old (i) 28 km N Atherton, 17°2'

145°26, 1 9, 21 Nov,, 87. (i) 22 km WN Ather-

ton, 17°7' 145°26', 1 2, 22 Nov., QM 700, NT,

(iii) 7 km SE Nourlangie Camp, 12°49 132°42',

19, 13 Junc, 64, (iv) 12 km S Nourlangie Camp,

1 of, 18 June, 85. (v) 185 km BE Darwin, 12°41'

32°55", 1 9, 14 June, 86, (vi) 17 km B Darwin,

12°29" 130°S9', I, 17 Sune, 531,

Notes: Localities i and vi were road kills, AU

lavalities Were low open grassy woodland.

Repeoduehon: (iii) 2 young born.

36, Conllurus penicillatus, Brush-tailed Tree-

rat

Localities: Nov’. (1) 7 ko SE Nourlangie Camp,

12°49" 132°42", 1), 13. June, 90, (ii) 9 km SE

Nourlangie Camp, 12"50° (32°41", 1 4, 19 June,

88, (ii) 10 km S Nowslangie Camp, 12°51,

132"41°, 1, 20 Tyne, 89.

Notes: Both Joculities were low grassy woodlund,

Reproductions (i) 3 young born,

37, Notomys alexis, Spinitex Hopping-ouse

Localities; Wa. (i) 14 km N Denham, 25°49'

113°32. 1 9 19 Apr, WAM M15290. Gil 14

km N Denham, 25°48 113731", 1 oy 1 &, 26-28

Apr., 166, 168. (iii) 160 km NE Carnarvan, | &,

13. 7 May, WAM M1529],

Noies: Caught in open seruh (i) and in tall open

shrubland (it), Bolh wreas were on red sand,

Judging from tracks in Jocality (7) and from syput-

lighting at locality (ii) N. alexis appeared to be

common at both localities,

38, Zyzamvs areures, Common Rock-tat

Localities: Gld (1) 22 km 8&8 Cooktown, 15°94"

145°13, 3 od, 4 Y& 7-9 Nev, OM 691, 2104, 95,

96, S34, WA. (ii) Forteseue River, 21° 18°

Hle'th d a 4 9 8 tune, WAM MUtS272. 107-

tid, (i) 165 km E Derby 17°6 125°10', 4 gy 5

“15-17 May, WAM MIS273-M1S286. (iv) 165

km E Derby, 17°7' (257°40', 3 &, & 2, 15-17 May,

W1, 104, 705, 543-548. (Vv) West Bustian above

Wyndham, 5°27° (28°27', | g, 1 9, 27 May,

WAM 15287, 100, Nu. fvi) 346 km 3 Bar-

win, 15°36 931°8', 19, 37 May, 9% (Yi) Nour-

langie Rock, 230 km EF Darwin, 12°81) 132°47%,

ig. Lb 2. 13 June, 97, 98.

Notes: The habitat of 4. areurusy canvol be des-

cribed by Specht's classification. ‘This animal

occasionally occurs on rocky slopes covered with

sparse Vegetation as in locality (iv) but more

often in rock piles devoid of vegetation (i, ii, iii

and v),

Reproduction: (i) Copulation plug present, (v1)

embryos in uterus.

Ectoparasites: (|, U, ith, iv) Leelaps pammorplus,

(i) Echidnephaga myrmecobi,

39. Zyzemys woodwardi, Large Rock-rat

Localities: N.7. (i) Nourlangie Rock, 230 km E

Darwin, 12°51" 132°47°, 3 dl 2 9, 2, 13 and 18

June, SAM M9899, 113-115. (ii) Cannon Hill

225 km E Darwin, 12°23’ 132°56', 4 2, 21 June,

116~118, 549.

Notes; Both localities are outlying scarps of the

Acnhem Land Escarpment.

Betoparasites: (i) Laelapy pammearphus.

40, Mastacomys fuscus, Broad-toothed rat

Loealiry: N.S.’ (i) Kosciusko Natl Pk, 36°23'

148°28', 49, 10-1! Feb, SAM M9897, AM

M10431, M1432, 77,

Notes: This locality ts a closed herbficid.

Reproduction: (i) 1 young born,

Ectoporasites: (i) Laelaps cyhbiala, Macropsyila

hercules, Pyviopsylla heplia.

41, Psetidomys delicatulus, Litthe Native-mouse

Localities: Old (1) 22 km SW Emerald, 23°41"

I48°4°, 2 oy 15 Dec, QM 2133, 14. WA, Cit)

189 km 8 Broome, 19°U" 121°145 1 9, 11 May,

59, N.T. (iii) 185 km E Darwin, '2°4l° 132°55',

19, 15 June, SAM M5898.

Notes: Cuught in low woodland (1) tall open

shrubland/hummock grassland (ii) and low open

Woodland.

Reproduction; (iii) 3 young born;

42. Pseudaniys novaehollandiae, New Holland

Mouse

Localities: N.S. (i) 30 km NE Newcastle,

32°3" 192"0", 2 d 4-9 Feb,, AM M10433. Vie.

(ii) 38 km E Sale, 38°h" 147°31° | 3, 23 Feb,

550.

Notes: Caught in closed scrub (i) and low open

woodlind/open heath (ily,

Reproduction: (i) 5 embryos in ulerus,

43, Pseudamys albocineteus, Ashy-grey Mouse

Localities: Widy (i) 22 km NE Jurien, 31°8°

tis’9", 2 df, 2 Y 12-1] Apr, WAM M15295,

25-27. (ii) Bernier Island, 24°56° 113°9', 2 ¥,

21-22 Apr., 28, 29,

66 1. F, ROBINSON EP AL.

Notes; Caught in closed heath (i) and low

shrubland on coastal dunes (li),

Reproduction; (ii) 4 young born.

Ectopuarisites: (i) Laelapy sp.

44, Preudomys occidentalis, Western Mouse

Localities: WA. (1) 17 km NE Bendering, 32°22"

1/8°28', 3 2 2 @ 3, 30-31 Mun, and 1 Apr.

WAM, M15294, M15305, 551, 552. (ii) L7 km

NE Bemilering, 32°21" 118°28', | dy 1 Apr, 553,

Notes: Canght in areas of tall shrubland,

Ecloparasites: (i, ti) Lrelups ap, tl) Srephane-

clrcws Th, Sp.

45. Psendomys pracconls, Shark Bay Mouse

Localities; Wo. G) Bermmier Id, 24°56" 113°9",

to. 2t Apr. WAM MIS5305, (il) Bernier Id,

24°58’ LIZ°R, Wd, 1 F, 21-23 Apr., WAM

Mi5306, 19, 554-556,

Notes: Cuught in Juw shrubland (<1) and tussock

grassland (ii) (Robinson er al, 97h),

Ectoparasites: (ii) Laclaps sp. (¥) Xenapsylla

vexabilis.

46, Psevdomys shortridgei, Shortridge’s

Native-mouse

Localities: Vie. (i) 42 km NE Hamilion, 37°31*

142°25°, 1 9, 4 Mar., 466, (il) 52 km NE Haril-

tun, 37°27" 142°28', 1 9, 7 Mar. 18.

Notes: Caught in areas of closed heath,

47, Pseudomys gracilicduddtus, Eastern Chest-

nut Native-mouse

Localities: Gla (i) 8 km SW ‘Townsville, 19°20°

l46°4 2 9, 8 Dec., OM 703, Gi) 26 km NE

Rockhampton, 23°19" 150°45", 2 of, 17-21 Dee.,

QM 727. Gili) 9 km NE Rockhampton, 23°20°

50°35, | 9, 8 Jan,, QM 2120, (iv) 98 km NW

Bundahere, 24°31" 151°28, 1 9 10 Jan, OM

211Y,

Notes: Caught in open grassy woodland (1), low

grassy WOodlabd (ii and iil) and low open forest

(iv).

Ectoparasiles: (iv) Laelups actla, L. nuiltalli-

48. Pseudoniys nanus, Western Chestnut

Nalive-mouse

Localities; Woda, fi) 165 km E Derby, 17°"

125"10, 4 f 2 9, 1, 18-17 May, WAM M15297,

M15300, M[5301, 435, 957-559. (ii) 248 km E

BDerhy, (7°7' 125°43", 2 & 1 2, 21 May. WAM

MIS3U2, 439-440), (Ui) IB km NE Kimberley

Research Station, 15°33" JIR"6', | 2, TB May,

444, N.7T. fiv) 346 km § Darwin, 18°34 13177",

19. 1 June, 445, (v) 7 kay SE Nourlangie Camp,

12°49" 132°42", | 9, 13 June, 258. (vi) i4 km S

Nourlangie Camp, 12°54 132°38', 1 9, 18 June,

473, (il) 1 km S Nourlangie Camp, 12°51

132°41', 1 G 20 June, 478.

Notes: Cyught in closed lussock vrassland (ft i

and lV), Open Woodland /closed tussock grassland

(i and it) add low grassy woodland (v, vi and

vil),

Reproduction: (i, iii) Independent

trapped, (iv, vi) 3 young born.

Fctoparasiles: (i, ji, iii, iv, v, vi) Laelaps «ella,

juveniles

49, Mus muaseulus, House-mouse

Localities: Qld (1) 32 km W Windorah, 25°20°

142°18', 1, 16 Oct. (it) 2 km NE Mt Isa, 1, 19

Oct, (iii) 25 km N Atherton, 17°39" 145°26°, 10,

2t Nov. (iv) I! km NE Atherton, 17°12’

145°33', 2, 21 Nov, (v) 22 km SW Emerald,

23°4l° 148°4" 7, 14 Dec. (vi) Nogoa River,

Emerald. 23°32° 148" 10°, §, 15 Dec. (viib 26 km

WE Rockhampton, 23°19 [50°45 % 19 Dee

(viii) 58 km N Maryborough, 25°6' 152°33', 7%

[4 Jan, N.S.W. (ix) 20 km SW Port Macquarie,

31°37" 152°50", 2, 2 Reb. (x) 50 km NE New-

castle, 32°39° 152°9°, 2, 4 Feb. AM M10421,

(ai) 20 km NE Mallacoota, 37°27) 149°57', 1,

17 Feb. Wic, (xil) 38 km E Sale, 38°6' 147°31',

15, 23-24 Peb, WA. (xiii) 17 km NE Bendering,

32°22" | 18°28", 22, 30 Mar—t Apr. (xiv) 32 km

S Hyden, 32°49° 119°, 7-10 Apr. (xv) 22 km

NE Jurien, 30°8’ 115°9', 9, 12 Apr, (xvi) [8 km

N Roebourne, 20°37’ 117°L1', 2, 9 May.

Notes: Mf. pusenlus was both widespread and

common. It was caught in tussock grassland (1),

coastal dunes (xii), grassy woodland (ii and viii),

closed grassland (iii, iv, v and vi), low grassy

woodland (vii), closed serub (ix), open forest

(x), Woodlund/closed heath (xi), closed heath

(ei) and (all serubland (xii and xiti),

50. Vromys canudtrecularus, Giant White-

tailed Rat

Localities: Qld (i) 23 km SW Portland Roads,

(2°44 143°14, 1 a, 31 Oct. 184. (ii) 19 km

SW Portland Roads, 12743" (43°17, | @, 1 2 2

Noy., 182, 183. (id) 32 kay S Cooktown, 15°45°

45°18 3 Sl, 7-9 Nov, fiv) 22 km S Cook-

town, 15°39" 145°13*, 1 a. 39, 5. 7-9 Nov. OM

696, (Vv) 22 km S Cooktown, 15°39" 145°14°. 1,

S Nov, (vi) 420 km SE Caivns, 17° 1S 1485°S6',

| fo. 1 4, 15-16 Nov., QM 2095, 191, (vii) 19

kin SE Atherton, 17°25' 145°31', 6d, 1 9, 25

Nov, OM 2096, TRX, 190 (vil) 3 km SE

Atherton, 17°20° (45°20, 1, 27 Nov. (ix) 14 km

FE Atherton, 17°15) 1745°97*, 1 2, 28 Nov,

Notes: All localities were in closed forest except

lecaliry (ivy where it was canght among boulder

heups close to patches ot closed forest,

Reproduction: (ii) | youn barn.

Ectoparasites, (ii, vi, vit) Laelaps sourheatt, tii)

Odantacerus sp, (WO) Pygiopsvila heplia,

$1, Meloniys cervinipes, Fawn-footed

Melomys

Localities: Qld Ci} 26 km SW Portlind Roads,

12°44 1439714) 2, 30 Det, (i) 32 km S$ Cook-

town, 19°45 148°19 3 43 9, 7-9 Nov. iii)

MARSUPIALS AND RODENTS IN AUSTRALIA 6?

4() ket SE Cairns, 17°1S' 145756 3 F. 15-16

Noy, (iv) 41 km SE Cairns, 17°15" 145556" 1 2,

15 Noy. tv) 19 km SE Atherton, 17°25" 45°31’,

1 9 25 Nov, (vi) 3 km SE Atherton, 17°20

14s°an, 1, 27 Nov. (vi) T2 km 8S Atherion,

16"28" 145°59, |, 1 Dec. (viii) 61 km N Rock-

hampton, 22°5)° 150°40°, 1 9. 5 Jan. fix) 98 km

NW Rundberg, 24°32" 181°28", 12, |2 Fan. (x)

38 km E Kingaroy, 26°39" 152°13, 1, 16 Jan,

Notes: All localities were closed forest,

Ectoparasites: (ii, iii) Laelaps mutralli, (ii, iti, iv,

Vv, vil, Gn) DL. rothsehildi, (vj Acarnthopsylla

incerta, (ix) A. pavida

52, Melomys littoralix, Grassland Melomys

Localines: @ld (i) 20 km SW Portland Roads,

12°44 143°16', 1 3, 1 Nov, (ii) 19 km SW

Portland Roads, 12°43° 143°17', | 9, 1 Nov. (ii)

21 km SW Portland Roads, 12°44° 143° 16, 2 8,

| Nov, (iv) 23 km S Portland Roads, 12°47'

143°18", 3 gd. 4 9, 23 Nov., QM 722. (y) 37

kn S Cooktown, 15°48" 145°1S*, 1 ot, 19, 2 Nov,

(vi) 22 km S Cooktown, 15°39" 145° 13,3 J, 1

@, 7-8 Noy. (vii) 17 kin S Cairns, 17°5° 145°47",

3 5,3 7, 14 Nov, (viii) 25 km WN Atherton, ¢7°3’

t45°26,, t oy - 3, 21 Nov, (ix) 11 km NE

Atherton, 17°12" 145°33° I dy 19. 22 Nov, (x)

22 km S@ Atherton, 17°22° 145°33', 4 J, 49, 29

Nov. (x1) 29 km SE Tanisfail, 17°46 146°7,

1 4 3 Dee. Gai) 6L km N Rockhampton, 22°52'

Psn'4p’, 2, 5 Jan. (xiii) 58 kin N Rockhampton,

22°52" 150741, 1 ot, 1 9, 5 Jan. (xiv) 58 km N

Maryborough, 25°8 152°32', 1 9, 14 Jan, (xv)

9 km SE Dunwich, North Stradbroke Ts., 27°32°

L53°30', 3 A 19-20 Jan. NLT. (xvid Nourlangie

Camp (205 km E Darwin), (246° 132°40', 1 2,

19 June, fxvii) 5 Km NE Darwin, 12°22°

AU S6 Fy 11 dune,

Notes: Muhbitats were closed forest (xvi), open

forest (xi, xii), low open forest/grassy woodland

G, ai, i, iv, sil, xiv), low grassy woodlund (y,

vi), low open grassy woodland (vii), closed grass-

Jufid (vint, WV), Closed sedyeland f%, xv, xviid

Ectoparasites: (vi, xvii) Leelaps nuttallr, Gi, iii,

iv, v, vi, vii. viii, ix, xi, xiii, xiv, XV, xvii) Z,

rothsehildl, (ix, xv) Mesolaclaps australferists,

(vil, 1X, x, IV, XV) Pugiepsylla leptin, Ge) &. sp.,

Acarnthopsylla incerta, A. pavida, Xenopsylla «anus-

traliaca, (ty ix) X. vexabilis.

53. Melomys spp

Localities: Qld (i) 62 kim NW Caen, 13°27’

142°57', 1 9, 29 Oct. QM 70%. (ii) 19 km SE

Atherfon, L7°25° 145°31, 1, 25 Noy., QM 721,

Notes: Habitats were riverine closed forest (1)

and closes! tovest (i).

Ectopamuites: (i) Laclaps rethschitdi, Gi) Pygice

pala sithatd, Acanthapsyta iecerta, A, pavida,

Nenopsylla australiaea.

Discussion

The results contain some significant distri-

bution tecords.

The Plague Rut Rettys villosissintur col-

lected 26 km SE of Wyndham is the second

and most northerly record from Western Aus-

tralia (Calaby 1974),

The Common Rock-rat Zyzomys areurus, @

Telatively common species in suitable habitat

in northern Australia, was collected 22 km S$

of Cooktown, which is the fourth and most

northerly record from Queensland (Tate 1952;

Gordon & Johnson 1973).

The Little Nalive-mouse, Pxeudonrys deli-

cati/as, collected 189 km S$ of Broome, is onc

of the most southerly records for this species

in Western Australia (Bannister 1969). The

record from Emerald, Queensland is further

intand than previous published records (Cova-

cevich & Easton 1974),

The Eastern Chestnut Native-mouse, Pyen-

domys gravilicaudalus, has recently “re-

appeared” near Townsville (Horsboom 1975).

Emerald (Taylor & Horner (1973) misidenti-

fied as P, australis ct, Mahoney & Posamenticr

(1975)) and north coastal N.8.W_ (Mahoney &

Posamentier 1975). Our data add three more

localities in coastal Queensland. This widely

distributed species appears to occur at a uni-

formly low population density, and consider-

able trapping effort has usually been expended

in its Capture (Mahoney & Posamentier 1975),

For comparison the trapping e(fart to capture

this species in the present study was} locality

(1) 60 trap nights, locality (ii) 330 trap nights,

locality (ili) 60 trap nights and locality (iv)

219 trap nights. Tt is, however, necessary to

take into account seasonal variations in popu-

lation density and this ig clearly not possible

in a study such as this, As an example, Tun-

ney’s Rat Ratrus tanneyi culmorum proved to

be extremely difticult to capture, an experience

also recorded by Taylor & Horner (1973).

One specimen was trapped at each of three

Jocalities in coastal Queensland but many

other localities were trapped in the hope of

capturing this rodent. One of these was

Archooceora State Forest, a Huop Pine plan-

tation im Southern Queensland where at certain

limes of ihe year ALt culimorum is abundant

and causes extensive damage to the Hoop Pine

Toot systems (Taylor & Harner 1973).

Although numerous signs of this species were

seen in the area ne rats were captured.

TWo rmfajor generalisations regarding the

Australian rodent fauna can be made as a

68 J. PF. ROBINSON FT AL,

TABLE 1

Trapping success for all species, tneluding Introduced

species, in the major habitat types sampled in eastern,

wesrerte and narthern Australia

Number Total Number Trapping

of trap of SUCCESS

Tabitat localities nights captures (%)

Closed forest 7 980 oY Wl

‘Tall open forest 2 138 55 39

Open forest 9 815 38 Wd

Woodland 17 20h 1a OU

Shrubland 6 765 83 10.8

Heath 1 Lo70 mm 10.5

Tussock ufassland Ww 13 64 8.9

Sedgeland 4 520 46 RR

Rockpiles 9 R50 45 1.6

result of this study covering a large proportion

of the habitat types over a wide area of Aus-

tralia:

(1) The trapping success in this study

(8.3%) supports Watts’ (1974) comment that

population densities of Australian rodents are

low in comparison with equivalent habitats

in the Northern Hemisphere. The highest trap-

ping success achieved was 55% in the Otwuy

Ranges, Victoria. Table | provides a broad

outline of the variation in trapping success in

the major habitat types sampled. The two

areas of tall open forest sampled proved to

support a substantially higher density of small

mammals than any of the other habitats. This

trend ig supported by trapping experience

(A. C. Robinson unpublished data) in other

areas of this habitat in Victoria.

(2) Australian small mammal faunas are

characterised by the low number of species

that occur sympatrically, In this stady sympat-

ric occurrence Was defined as occurrence on

the same 200 m trapline, bearing in mind that

attempts were made to keep each trapline in

a single major habitat,

Of thirty-nine instances of sympatry noted

the largest number of species occurring to

pether was four (Table 2), Most cases involve

species occupying obviously different eco-

logical niches by virtue of such factors us:

(a) size differences, eg. Rartus leucopus,

Urontys caudimacularus, (b) above ground

nests compared with burrows, c.g. Melomys

linorally, R. sordidus, (¢) insectivorous mar-

supials compared with omnivorous rodents,

Le. Antechinus stuartii, R. fuscipes, (d) intro-

duced species with native species, eg. Mix

musculus, Pseudamys accidentalis, Only three

cases Which may indicate soine degree of com

TABLE 2

Sitall nianimal species occurring together in the same

200 nt trapline. Most abundant species shown first:

locality number refers ta thiy species in the body vf

the paper

Lueality

Zev)

‘Sympatrie specics

Ratius villosissinus, Mus musculus

29(i) R. leucopus, Urowys caudimaculatus

26(0\) R_ yardiduy, Melomys litferalis, Sminthopsis

rufigenis

AR(i) Zycomys argurus, U. caudimaculaus, M-

cervinipes

26(iv) RR. serdidus, M, littaralis, R. ratty

330) At, eervinipes, U. candimaculatus, R. rartur

24i1) RL fuseipes, M. cervinipes

26(vi) RR. sordidus, R, rarnes, Muy trusculius

SUV) AM. cervinipes, U. caudimaculatis

24(1) RK. fuscipes, Uy caudimeculatus

26(v) = -R. sandidus, M. littoralix

Viv) Jseaden macrourus, Pseudomys pracili

candatus

324i) R, tunneyi, Mus musculus

32¢1) Mis musculus, P. delicatilis

320i) RR. tunneyi, M. litteralis

ATi) PP, owracilicunedatus, M. litteralis

12(4) Perameley nayuta, My cervintipes

(t(vi) Ll. maerourtis, M. littoralis, R, retinas

250) = -R, lutreolus, Antechinus stuartii, J.

HAC FONTIUR

33(ix) RR. raties, P. novaehollandiae

RUN) OR. ratius, Re fuscipes

2iv) RK. Jaseipes, A, swainsorii, Mastacomys

Jusenys

2iv) RR. Juscipes, A, swainsunit, A, stuart

Divi) Ry fuseipes, AL stiartii, Mas miuseulus

23x) ORK, fuscipes, A. stuart, A, swarinsonti,

Poiorous tridactylus

49(xi1) Me mtseulis, BL novaehollandiae

Zvi) Ry liirealius, A. stiartii, 1. obesnlus

Jax) OR, fitveipes, A, wtartii, A. swainsonii

Diasili) KR. fuseipes, A wtuaridi, A, swainsenti

WO(vili) 4. titer, Ry Intreolus, A, swainsonit

24(x) KR. ltarreolus, I. sharcridget

49( sil) Mus onisentias, Py aeeidentalis

a5(i) Pr. pracconis, 2. -albecinereus, Perameler

boaucainville

qa RR. tteneyi, Po narrits'

Aiv) Ry, tenneyi, Po mans

Sid) OR. tunnent, R. villosissinrus

27) OR, eallenti, M. littaralis

B1(si1) Ro tanent, My littoralis

W(v) AL belins, 1. macrourus, Dasyurus hallneatas

petition between species Were noted. (a) In

locality 26(iv) [7 km S of Cairns, Qld, R,

rettus and R. serdidus occurred together. This

was an area of disturbed open woodlaund ad-

MARSUPIALS AND RODENTS IN AUSTRALIA 69

jacent to cane fields arid tay bave represented

an unstable situation. (b) In locality 33(ix)

40) knit N of Newcastle, N.S.W., R. ratte and

R. fuselpes occurred toyether. Again this was

an drea of open forest adjacent to heathlands

regenerating from sand mining and may have

been an Unstable situation. (¢) In locality

31(v) 26 km FE of Wyndham, W,A., R, tin

nevi and R_ villesissimus occurred together,

This Was the edge of a flood plain supporting

a closed tussock grassland adjacent to an open

grassy woodland and may have been part of

wn ecotone.

Some previously unknown forms of ecto-

parasites were collected and some consuler-

thle range extensions were recorded. ‘The fleas

included a new Stephanecireus from PL oeei-

dentalis, \\ new Pygiapsyla tram Rf. assimili¢

and i new subspecies of Pygiopsylla ratnhowil

from R. ruttuy and Ry serdidus, The mites in-

cluded a new Luelups from P. eceidentalix, a

new Luelaps from P. praceonis ind possibly

also P. albacinerens.

Acknowledgments

We wish lo dhawk the South Australian

Nahonal Parks and Wildlife Service, the

Western Australian Department of Fisheries

and Wildlife, the Northern Teritory Adminis-

tration, the Fauna Board of the Queensland

Department of Primary Industries, the Queens-

land Forestry Department, the New South

Wules National Parks & Wildlife Service and

the Victorian Department of Fisheries &

Wildlife for providing the various permits

required and for greatly facilitating ihe work

in other ways, We would particularly like to

thank the Western Australian Wildlife Author-

ity for permission to Irap on Bernier Island.

Ectoparasites were kindly identified by: Prof,

R, Traub, University of Maryland (fleas); Dr

R. Domrow, Queensland Institute of Medical

Research (mites); and Dr D, Kemp,

C.3.1.R.0, Division of Animal Health (ticks)-

Particular thanks go to the numerous people

throughout Australia without whose help this

irip would not have been possible. In Queens-

land—B. Allen, R. Allison, J. Barrett, A.

Borsboom, J. Boyrke, P. Brownell, M. Cassells,

J, Covacevich, G. Gordon, G. Ingram, P.

Johnson, P. Krauss, C. Limpus, D, Morris, D.

Matthews, I. Pack, J. Roberts, K. Sparks, F,

Stecne, B, Voerman, J. Winter and M.

Weaver; in New South Wales—A, Fox, A,

Jelinek, D, Lunney and C. Jidemane, io

Western Australia—G, Fuulkner, D, King, J.

Rocchi, L. Sylvester and §. Whitchouse; in

Northern Territory—R. Begg, D, Lindner, P.

Latz, G. Miles, D, Morgan, M, Parker and F,

Whorle.

The study Was. finaheed by a grant from the

Australian Biological Resources Survey

Intennm Council.

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pials in Western Australia. J. R. Soc. W.

Aust. 19, 17-32.

Gorpon, G. & JoHNnson, P. M. (1973) Rock rat

in north Queensland. Qld Agric. J. 99, 2-3.

Harrison, J. L. (1961)Mammals of Innisfail. 1.

Species and distribution. Aust. J. Zool. 10,

45-83.

Jounson, D. H. (1964) Mammals of the Arnhem

Land expedition. Jn R. L. Specht (Ed.)

“Records of the Australian-American Expedi-

tion to Arnhem Land”. Vol, 4, pp. 427-515

(Melbourne Univ. Press: Melbourne).

Manoney, J. A. & PosaMENTIER, H, (1975) The

occurrence of the native rodent Pseudomys

gracilicaudatus (Gould 1845) (Rodentia:

Muridae), in New South Wales. Aust. Mam-

mal. 1, 333-346.

Marrow, B, J. (1958) A survey of the mar-

supials of New South Wales. C.S.LR.O-

Wildl. Res. 3, 71-114.

ParKeER, S. A. (1973) An annotated checklist of

the native land mammals of the Northern

Territory. Rec, S. Aust. Mus, 16, 1-57.

Rie, W. D. L. (1970) “A guide to the native

mammals of Australia” (Oxford Univ. Press:

London).

Rosinson, A. C., Roprnson, J. F. & Watts,

Cc. H. S. (1976) The Shark Bay Mouse

Pseudamys praeconis and other mammals on

Bernier Island, Western Australia. West.

Aust. Nat, 13, 149-155.

Specut, R. L, (1970) Vegetation. In G. W.

Leeper (Ed.) “The Australian Environment”

(C.S.I.R.O.: Melbourne).

Sprecut, R. L., Roz, E. M. & BroucHTon, V. H.

(1974) Conservation of major plant com-

munities in Australia and Papua New Guinea.

Aust. J. Bot. Suppl. Ser. No. 7, 1-647.

Tate, G. H, H. (1952) Results of the Archbold

Expeditions No. 66. Mammals of Cape York

Peninsula, with notes on the occurrences of

rain forest in Queensland. Bull. Am. Mus.

Nat, Hist. 98, 563-616.

Taytor, J, M, & Horner, B. E. (1973) Results

of the Archbold Expeditions No. 98. Sys-

tematics of Native Australian Rattus (Ro-

dentia, Muridae). Bull. Am. Mus. Nat. Hist.

150, 1-130.

Watts, C. H. S. (1974) The native rodents of

Australia: a personal view. Aust. Mammal,

1, 109-116,

Watts, C, H. 8, (1977) The foods eaten by some

Australian rodents (Muridae). Aust. Wildl.

Rey. 4, 151-157.

Woop-Jones, F. (1923) “The Mammals of South

Australia” (Govt Printer: Adelaide).

STRUCTURE OF THE WILLOCHRAN BASIN, SOUTHERN FLINDERS

RANGES, SOUTH AUSTRALIA

BY B. E. MILTON & C. R. TWIDALE

Summary

Interpretation of seismic refraction data obtained on four east-west lines across the Willochra Basin

suggests that the structure is bounded on its eastern and western margins by north-south trending

faults which delineate a long narrow downfaulted zone. Thus as O’Driscoll (1956) suggested the

Willochra Basin is occupied by a graben or rift valley, developed in the crest of a major anticline.

Two types of Precambrian basement rock can be identified beneath the Cainozoic basin deposits

which have a maximum thickness of some 250 m.

STRUCTURE OF THE WILLOCHRA BASIN, SOUTHERN FLINDERS

RANGES, SOUTH AUSTRALIA

by B. E. Mizton* and C. R. TwipALet

Summary

Miiron, B. B. & Twroace, C. R- (1978) Structure of the Willochra Basin, southern Flinders

Ratiges, South Australia, Vrans. R. Soe. 8. Aust. 102(3), 71-77, 31 May, 1978.

Interpretation of seismic refraction data obtained on four east-west lines across the

Willochra Basin suggests that the structure is bounded on its eastern and Western margins by

north-south trending faulls which delineate a long narrow downfaulted zone. Thus as

O'Driscoll (1956) suggested the Willochra Basin is occupied by a grahen or rift valley,

developed in the crest of i major anticline. Two types of Precambrian basement rock can

be identified beneath the Cuinozoic basin deposits which have a maximum thickness of some

250 m.

Tatroduction

The Willochra Basin (Fig. 1) is an inter-

montane basin eroded in folded Proterozoic

Adelaide System strata and partially filled with

Cainozoic lacustrine and alluvial sediments,

Occupied by the Willochra plains and drained

by the intermittently flowing Willochra Creek

and its several tributaries, the basin surface

stands about 335 m above sea level in the south

and gently slopes down to about 200 m eleva-

tion at its northern extremity.

The flat aggradational plains are underlain

by up to 170 m of unconsolidated fat-lying

sediments in the northern half of the Basin and

by up to 250 m in the south. They rest

unconformably on a broad, gently sloping and

only slightly irregular surface eroded in the

Proterozoic sediments, In the south Quaternary

alluvium fests directly on the Adelaidean rocks,

bul in the north Up to 15 m of Eocene lake

beds intervene. The latter are fine-grained in

the basin proper and im marginal exposures

near Simmonston (Miles 1956), but consist of

quartzite and conglomerate in the lower Mount

Arden Creek Valley and in the valleys of the

Kanyaka and Wirreanda creeks (Shepherd &

Thatcher 1959; Webb & Von der Borch 1962;

Twidale 1966; Binks 1971).

These Caihozoic sediments are essentially

restricted to am elongate, natrow, north-south

depression exlending from the vicinity of Mel-

rose as fur horth as Gordon, There is con-

siderable overlap of the Quaternary alluvia

which extend up major valleys, but the thicker

sequences are apparently confined to a long,

harrow trough.

The nature of the deeper basi or trough

has been the subject of mild controversy for

some years. O'Driscoll (1956, p. 11) specu-

luted that the Basin occupies a graben, He

delineated a fault in the eastern side of the

Basin but to the west the only faulting he could

cite In support of his contention is located in

the ranges well away from the area under dis-

cussion. More recent and conservative opinion

has been that the topographic basin occupies a

denuded anticline characterised by relief

inversion (Shepherd & Thatcher 1959, p. 14;

Twidale 1966, p. 8).

However, during the course of geophysical

traverses undertaken in connection with pedi-

ment studies and designed to determine the

shape of the pre-Cainozoic surface, that is, the

surface cut in the folded Adelaide System strata

where it plunges beneath the basin sediments,

evidence has come to light which though it still

docs not incontrovertibly prove, nevertheless

strongly suggests, that O'Driscoll’s intuitive

guess was correct and that the Willochra Basin

indeed occupies a north-south irending graben.

* Department of Mines and Energy, P.O. Box 151, Eastwood, S.A, 5063.

} Department of Geography, University of Adelaide,

72 B, E. MILTON & C. R. TWIDALE

TABLE 1

Velocity analysis

WI75A

SP 100—113

523] m/s

225

SP 114—130 | SP 131-133

4545

283

WI75C

SP 10—16

5003

167

rT)

aa]

BASIN MARGIN

WI76A

SP 15—22 | SP 23—53

5 18

4776 5203

297 352

No. observations (n)

Drn D.E.

Geophysical Operations

Seismic Recording Procedures

The location of seismic traverses along which

refraction data were obtained is shown in

Fig. 1. Profiles WI75A, B and C were shot in

1975; WI76A in 1976. Detector intervals were

61 m or 30.5 m, with continuous coverage

except on line WI75B. Detectors were laid

in-line with the energy source, the location of

which relative to the detector array was

Average velocity (V)

SP 55—80

4735

171

SP 81—100

Standard deviation (s)

S—13198 S.A. Dept. of Mines and Energy

designed to record the basement refractor,

Information on near surface material was

obtained from refraction spreads with a detec-

tor interval of 9 m and shot every 1460 m.

Seismic Computing

Information extracted from the seismic data

measures depth relative to mean sea level to

a refracting horizon and velocity along the

interface, “Time-distance’ curves are con-

structed by plotting arrival times at individual

PORT AUGUSTA

Fig.

STRUCTURE OF THE WILLOCHRA BASIN 73

PARACHILNA

L Torrens

WILLOCHRA

BASIN

PY AUGUSTA\W

WILMINGTON

AE TERBOROUGH

ADELAIDE

& Diapiric breceja.

a! Stratigraphic welts.

Seismic line.

Line of demarcation of

basement velocities.

—— Basin margin.

a\ \

i REMARK ABLE a

| \ ~

| Vy) -——-~ Modified basin,

Faults,

_-ap— Gravity contours

=“ (milligalls)

Okm 5 10 15 20 25

[a re an er

YS,

\ \\ w\

1 | \

yy) \ oRROROO

1. Bouguer gravity anomalies and structure of the Willochra Basin, with locality map inset.

74 B, E. MILTON & C. R, TWIDALE

detectors against their distance from an energy

source. If the assumption is valid that the

velocities Within seismic strata are constant, the

plotted points fall on straight line segments,

Depths to refraction horizons below detector

locations, other than the near surface seismic

events, were computed using a method des-

cribed by Hawkins (1961), Velocities were

obtained by measuring the inverse of the slape

of the straight line segments.

Velocities from observed data in this project

have, except for shallow horizons for which

reciprocal information is not available, been

computed using the “method of differences’.

Provided the dip component of the refracting

horizon along the seismic line does not change,

the value so determined should contain a small

error term only,

Depth calculations using Hawkins’ method

involve velocity and time terms, hence are sub-

ject to greater errors than velocities, For

example, if basement Velocity values have an

error of = 5% and refraction times + .002

second, depth computations relative to datum

could be in error by between 7% and

8%. It is considered that this error value

applies approximately to depth calculations of

the bedrock refractor in the Willochra Basin.

Velocity Analysis

Velocities computed for the bedrock horizon

along the seismic traverses appear to fall into

regular groupings, as shown in Table |,

Bedrock velocities from spread WI75B are

based on a very limited number of

observations. They average about 5200 m/s

and fit into the second column on Table |,

‘The basin appears to be bounded by faulting

on the eastern and western margins, but it is

also upparent thar a chunge in bedrock

velocity occurs near the centre of the basin on

line WI7SA atid fear the easter margin of

the basin on WI76A, The significance of the

change is discussed in a later section,

The jear-surface material withii the basin

has a range of velocities from 300 to 800 m/s

and a thickness of about 2 to 3 m. This layer

has been omilled from the cross sections to

avoid confusion. A possible water table velocily

of around 1500 m/s has been recorded at some

locations, e.g. wear the western end of line

WIT75A, It also occurs crratically on line 76A,

bul has not been plotted because of its shallow

depth of about 7 to 9 m below ground surface.

Below these events lies a refractor with the

following, velocity characteristics:

TABLE 2

Clay hartum velocines

n V s

WITS5A: SP 101-130 «26 «61913 m/s 153

W175C; 1b 16 5 2886 352

WLIGA: 23-60 438 1890 45

WLISB: 103-114 2 T1968 |

71 «1922 m/s 143

Captions 48.14 Table [,

This horizon has a depth ranging from about

6 to nearly 20 m and probably correlates with

the upper surface of a mottled cluy series,

dated as Recent or late Pleistocene. The fairly

wide variation of velocities could result from

varying percentages of sand, calcite, ete.,

although lack of reciprocal refraction coverage

in many instances reduces the precision of

velocity measurements.

Intermediate velocities. between the clay

honzon and basement can he seen on the

WI75B and WI76A sections. Average valyes

of these und bedrock velocities, the latter

divided jmto eastern and Western groupings,

are:

TABLE 2

Sasementand intermediate herizon veloeltics

Basement, easiern mm mr ne 34 V = 4681 m/s s = 743 & = 25 g/ems

Basement, western i i= 44 Vo = 5196 s = 296 Fe 2.6 g/ems

Intermediate | 7 os n= 5 V = 359% § = 222

Intermediate IT n= 2) v — 29! s = 268

Abbrevianons os im Table 1,

Equivalent specific gravity values have been

computed from velocities using graphical

relationship between density und velocity

(Drake in Grant & West 1965, p, 200) for use

in jnterpreting gravity patterns. The curve

does not give reliable values of density for the

Adelaide System rocks, but as density “ontrarty

were used to calculate comparative gravity

values, i wos considered that these would be

rensonable,

Gravity Dala

Gravity expression of the basin can be seen

on the western third of ORROROO | :250 000

STRUCTURE OF THE WILLOCHRA BASIN 75

sheet. of which a Houguer contour map was

published by the South Australian Department

of Mines in 1975, This map is based on data

fram a helicopter survey undertakea for the

Bureau of Mineral Resources by Wongela

Creophysical Pty Ltd in 1970 (Tucker &

Brown 1973)! with stations on a grid spacing

of aboul 7.2 km, and on ground data from

South Australian Department of Mines surveys,

Figure ( is a contour map at 1 milligal intec-

vals of Bouyuer gravicy, with station locations

shown In the figure,

Contours of residual gravity were obtained

by deducting a 7egional surface from the

Bougtier contour map. Patterns do not vary

significantly on the Boupuer and residoal maps

sud the former only has been included here.

Residual values reveal a total anomaly of

between ~ 6 and 10 mifligals and the entire

residual pattern is superimposed on a large

gravity low extending from the southem part

of BURRA, through ORROROO to the

northert limit of PARACHILNA, a dis-

jance uf ahout 350 km, This has a total

res;dual anomaly of about ~ 25 milligals and

ils origin is considered to be a deep, low

density block tn the pre-Adelaidean rocks

(Tucker & Brown 1973),

Basin margins

Al the western extremities of seismic lines

WI7SA, WI75C and WIT6A (Fig, 2), faulting

of the high speed (basement) retractor is in

hear coinenenee with the western murgio of

the basin as mapped by O'Driscoll, The faults

have a throw of between 100 m and 150 m,

although the seismic data are not easily inter-

pretable on the northerunsost two lines, On the

eravity maps, the lo¢ation of the basin margin

can he traced approximately to the north of

line WI7SA, bur ts less evident to the south

of that line. This reflects the composite origins

of the gravity patterns to which variations of

density of the Adelaide System rocks contri-

bute, as well as the conlrast helween low

density basin sediments and basement racks.

Although the basin shows as an area of low

pravity Values, its boundaries sre not, in

general. clearly defined. An exception is the

gravily expression of the Simmanstoa Fault

which forms the northern margin of the basin,

bver most ot which there is a clearly defined

gravity pradient to the south,

The castern margin is more complex in tls

geophysical expression than the western or

northern boundaries. On seismic line WI7SA

a basement fauli. with a throw of abour 50) m

represents the basin limits, and O’Driscoll's

tentative margin has been adjusted on Fig. 1

to pass over the fault. On line 76A, however,

a basement fault of about 75 m which appears

to correlate with the fault on 75A, lies well to

the east of the basin margin. The correlation

of the two faults rests on the similarity in

seismic velocities on either side of cach fault

and the (residual) gravily pattern, and is also

indicated on Fig, 1, The margin interpreted

by O'Driscoll coincides with a small basement

fault on line 764A at shot point 54 (Fig. 2),

but the congistency of the seismic section

suggests that the limit of the basin sediments

lies around shor points 60-61, i.e, about 2.2 km

further east than indicated by the water well

lays.

As at the western boundary, the eastern

murgit is reflected as a component of gravity

patterns, but is difficult to extract Fron the

total effect.

Basin fill

In the busin no seismic events were reeorded

between the Recent Pleistocene clay horizon

referred to in the section on velocity analysis,

and the basement refractor, This clay layer

persists campletely across the basin on all

traverses shot Te has an equivalent density

value of ahoul 18 ¢/crn, which has been used

in gravity analysis in the section on “Basement

rack types”.

The near surface, “weathering” horizons and

an intermittent water table event have been

briefly described above.

Bedrock configuration

The physical contrasts between the sedimen-

tery fill and bedrock, even where moderately

Weathered, are quite sharp. The seismic breaks

are accordingly of good quality and mapping

of the basement surface is considered to be of

fair accursey, subject to the error terms dis-

cussed above, Depth to bedrock bhelaw surface

ranges from around 50 m on the eastern end

of WI75A to ahoul 250 m on WI75B

Although the data on ihis line are of poor

quality, duc to limited eoverage, there is some

confirmation of this maximum recorded thick-

\ Tucker, DD YW. & Brown, F. W, (1973) Reconnaissance helicopier gravity survey la the Flinders

Ranges, South Australia, 1970. Rec. Bur. Miner, Resuur. Geol, Geogphys. 1873/12 (unpublished),

130

125

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76 B. E. MILTON & C. R. TWIDALE

ness in the presence of a gravity low, which

could result from a thicker section of low

density material,

The basement surface over the seismic

sections shows a slight increase in depth from

east to west, with minor faulling and small

scule structure being recorded as shown in Fig.

2. Some of the undulations could be the result

of variations in thickness and degree of

weathering of the bedrock. The overall change

in depth to bedrock contributes significantly to

gravity patterns within the basin, but the effect

of minor faults and structure is unlikely to be

of sufficient magnitude to detect on the gravity

contours,

Basement rock types

The change in basement velocity shown in

Table 1, could result from variations of

weathering, or from changes in rock type. The

latter is considered more likely because of the

division into two discrete groups with a sharp

discontinuity, with weathering effects having

4 minor influence on velocities. It is estimated

that the observational error of the velocities is

about 5%; the range of velocities recorded in

cach case is about 10%, the difference prob.

ably being accounted for by differential

weathering of bedrock.

Atv examination of drillers’ logs from water

wells and geological logs from three

stratigraphic wells drilled in the basin

tentatively suggests that basement material

ussociated with higher velocity, ie. west of the

ling shown on Fig, 1, consists of slate, while

that to the east of the line appears to cansist

of siltstones, quartzite and shales,

Gravity anomalies withia the basin consist of

lows. in the north and central part and a west-

northwest trending ridge in the south central

area, It is considered that the source of the

residual patterns has two major contributors,

viz, the densily contrast between Tertiary and

younger sediments and bedrock, and changes

in basement rock types, as discussed above.

The degree of weathering of basement may

also contribute in a minor fashion to the

anomalous patterns.

Assuming density values of the two hasetnent

types of 2.5 and 2.6 g/cm", and of the sedi-

mentary fill of 1,8 g/cm®, an approximate

effect on gravity patterns can be obtained,

Along the northern seismic fine, WITSA, the

2 Milton, B. E. (1977) Geophysical exploration of the Willochru Basen. S$. Aust Dept.

Unpubl. Rept, RB 77/79.

variation in prayity vahies due to the change

in basement density over a distance of 7.5 kin

is abow 6 milligals, provided that this line

segment is centred on the change m rock type.

Over the same part of the seismic line, the con-

wibution to gravity values due ta changes in

thickness of the sediments from less than 100

to 150m, would amount ta between [4+ and 3

milligals. The sum of these ts suffictent to

account for most of the gravity anomaly along

WI7S5A. If this explanation of the gravity

patterns is valid, distribution of the two types

of bedrock can be extrapolated north and south

of the seismic line from a consideration of the

residual gravity contours, The line of demnarea-

lion of the two bedrock velocities is shown on

Fig. 1.

However, this simple analysis cannot he

applied along line WI76A due io a complex

distribution of sediments of varying densities

between the surface and basement over the

eastern half of the line, as indicated in Table

3. The implications of these observations are

discussed by Millton®,

Discussion und Coneclasions

The abrupt breaks of slope in the pre

Cainozoic bedrock floor demonstrated by the

geophysical traverses are best interpretec! ws

Fault scarps, though only drilling can really

demonstrate their character. Altermative

explanations of the steep scarps are not

accepted for the following reasons, The

lithology and disposition of the Proterozoic

strata exposed at the edge of the Basin an¢

probably giving nse to the strony refraction in

the area of the subsurface scarps is not such as

to promote the development of escarpments of

cither the steepness or clevation of those

recorded by the survey. Nor are the strata and

stratigraphy of a type or structure conducive

to scarp retreat (see Tricart 1957; Twidale

1960, 1967): there is neither a really resistant

formation, nor are the strata flattying., Te

interpret the searps as river bluffs demands

that all three traverses were quite fortuitously

located over the points where the pre-Tertiary

Willochra Creek impinged upon the valley sides

to produce river cliffs; and this is asking much

of coincidence,

On the other hand, if the scarps are

interpreted as of fault ongin their steepness is

readily comprehensible. ‘The readings to the

Mines,

STRUCTURE OF THE WILLOCHRA BASIN 77

west of shot point 100 on line WI7SA are

confused, probably because the traverse was

inadvertently located above a deep valley cut

into the fault scarp—a feature commonplace

on modern fault scarps such as those bounding

Death Valley, California. If this interpretation

is correct, the profiles of the floor eroded in

Adelaidean sediments obtained on the three

northern seismic. lines (Fig. 2) indicate that

the central part of the Willochra Basin, at least,

is a graben structure, and that the Cainozoic

sedimentation has been controlled by the

marginal faulting.

It is not uncommon to find a graben deve-

loped in the crest of an anticline (see, e.g.,

Latitte 1939: alsa Twidale 1971, pp, 120-131,

esp. p. 129) and indeed one of the oldest and

most widely favoured theories concerning the

origin of wrahens, that due to Gregory (1921),

calls for the structure developing in such areas

of tensional stress, The structure is essentially

of pre-Terhary age, for there is no evidence of

significant dislocation of the Cainozoic strata

along the lines of fault, though Eocene lake

beds in ibe gencral region have been faulted

(Webb & Von der Borch 1962). However,

there is ample evidence of contemporary seis-

mic activity at both margins of the postulated

graben, but especially on the western side of

the structure (Sutton & White 1968, pp.

27-29).

The Willochra Basin in thus essentially a

graben. The structure is deeper in the west

than in the east and may be more actively

subsiding on the western than the eastern

flank, again comparisons can be made with the

modern grabens, like Death Valley, which are

tilting as well as subsiding (Hunt & Mabey

1966).

Acknowledgements

The writers thank N. H. J. Frith, now of

Esso (Australia) Pty Ltd who directed the

seismic field work und also interpreted the

1975 data. The work described here was

financed by funds from an A.R.G,.C. award

and from the South Australian Department of

Mines, The paper is published by permission

of the Director of Mines, South Australia.

References

Hinks, Py J. (1917) The geology of the ORRO-

ROO 1:250 000 mup area, Rept. Invest. geol.

Surv. 5S, Aust, 36,

Gant, FS. & Wesr, G. F. (1965) “Interpreta-

tation in applied geophysies. (McGraw-Hill

Book Co., New York).

Grigamy, J, W. (1921) “The Rift Valleys and

Geology of East Africa.” (Seeley, Service

and Co., London),

Haweins, F, V, (1961) The reciprocal method

of routine shallow seismic refraction investi-

gations. Geophysics, 26, 806-819.

Hunt, C, B, & Masey, DB. (1966) Stratigraphy

and Structure, Death Valley, Californii.

Prof, Pap, U.S, geol, Surv, A9deA,

Larrrre, R. (1939) Bbide géologique de I'Aures.

Bull. Sery. Carte Géol. Alger. (2¢ Séries

Siratie. Deserip. Rex.) 15.

Mins, Ko R. (1956) Clay deposit at Simmonsion,

Min, Rev, Adelaide, WO, 34-35.

O'pRiscoLt, FB. F, D. (1956) Hydrology of the

Willochra Basin. Rept. Invest. geal, Surv. S.

Aust, 7.

SHupHerp, R. G. & THATCHER, D. (1959) The

geology of the Quorn Military Sheet, Rept,

fnvest. geol, Surv, 8. Aust, 20.

Sutton, D. J. & Wire, R. E. (1968) The seis-

micity of South Australia. J. geal, Soc, Aust,

15, 25-32.

TricarT. J. (1957) L’evolution des versants, Jn].

géogr., 108-115.

Twipate, C. R, (1960) Some problems of slope

development. J. geol. Soc. Aust. 6, 131-148,

TwinaLe, C. R. (1966) Chronology of denudation

in the southern Flinders Ranges, South Aus-

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Twipae, C. R. (1967) On the origin of the pied-

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J. Geol. 75, 393-411.

TwipaLe, C. R. (1971)

(Canberra).

Weng, B. P. & Von per Borcu, C. (1962) Wil-

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1;63 360 Series, veol, Surv. S. Aust,

“Structural Landforms.”

NEMATODE AND OTHER HELMINTH PARASITES OF THE KANGAROO

ISLAND WALLABY, MACROPUS EUGENII (DESMAREST).

2. SITE SELECTION WITHIN THE STOMACH

BY LESLEY R. SMALES AND PATRICIA M. MAWSON

Summary

Stomachs of 99 Kangaroo Island Wallabies were divided into regions. The anterior 4/5 of the

stomach appears to be analagous to the rumen while the posterior 1/5 corresponds to the abomasum

of the sheep. Nematodes present were identified and site preferences determined.

NEMATODE AND OTHER HELMINTH PARASITES OF THE KANGAROO

ISLAND WALLABY, MACROPUS EUGENI! (DESMAREST), 2. SITE

SELECTION WITHIN THE STOMACH

by Lestey R. SmaAves* and PatriciA M. MAwson*

Summary

SMALes, L. R. & Mawson, P, M. (1977) Nematode and other helminth parasites of the

Kangaroo Island Wallaby, Mucropus eugenii (Desmarest), 2. Site selection within the

stomach, Trans, R. Sou, 8, Aust. 102(3), 79-83, 31 May, 1978.

Stomachs of 99 Kangaroo Island Wallabies were divided into regions. The anterior 4/5

of the stomach appears to be analagous to the rumen while the posterior 1/5 corresponds 10

ihe abomasum of the sheep. Nematodes present were identified and sile preferences

determined,

Introduction

The stomach, caecum, and colon of many

herbivorous hosts offer an environment capable

of supporting a number of closely related

nematode species. Such species flocks have

been described for the rhinoceros and ele-

phant (Chabaud 1956), tortoise (Schad 1963;

Petier 1963) and kangaroo (Mycylowycz

1964). Holmes (1973) has shown that nema-

todes actively chose preferred sites within the

host. Species flocks are able to exist in a host

because each member species occupies a

different ecological niche. These niches can be

separated by spatial, behavioural or temporal

characters,

The nematode Labiostrongylus eugenii

occurs in the Kangaroo Island Wallaby

(Maerepus ejigenii), A survey undertaken pre-

liminary to a study of the life history of this

nematode (Smalest) revealed the presence of

such a species flock in the stomach. During a

subsequent epidemiological survey of the

nematodes (Smales & Mawson 1978), an

opportunity was provided to study the ecology

of the species comprising this flock. Spatial

distribution in the stomach Jumen was

investigated, and some observations made on

the feeding behaviour and seasonal occurrence

of cach species.

In addition the site preferences of the

developmental stages of FL. eugenii were

defined.

Methods

The general gross and microscopical

appearance of the wallaby stomach was

examined and found to resemble that of the

Red Kangaroo (Megaleia rufa) as described by

Grilliths & Barton (1966) (Fig. 1).

Ninety-nine male wallabies were taken at

two monthly intervals, between April 1973 and

March 1975 from Kangaroo Island, South

Australia, The collecting areas and methods of

capture used have been described (Smales &

Mawson 1978).

At post mortem the stomach of cach

wallaby was carefully removed and ligatured

so that it was divided into the following four

regions:

1. The cardiac end of the saccular stomach

including the oesophageal opening.

2. The central section of the saccular

stomach.

3. The pyloric end of the saccular stomach

including the non-saccular region,

4. The gastric pouch and pylorus.

The contents of cach section so formed were

treated separately, by sieving through bolting

“Department of Zoology, University of Adelaide, North Terrace, Adelaide, S. Aust, S000,

1Smales, L. R. (1976) A study of the biology of a nematode Labiostroneylus eugenil (Johnson &

Mawson) parasitic in the stomuch of the tamymar wallaby (Macropus cugenii Desmarest). Ph.D,

Thesis, University of Adelaide (unpublished).

80 LESLEY R. SMALES & PATRICIA M. MAWSON

Fig. 1. Stomach of wallaby, showing positions (dotted lines) where ligatures were placed. Numbers

indicate sections referred to in text. O, oesophagus; IN, anterior end of intestine.

TABLE |

Mean measurements from 20 wallabies of the pH

values in three parts of the stomach

pH => $.D. Range

saccular stomach 6.99 + 0.5 6.3 - 7.8

non-saccular stomach 6.7 + 0.7 5.5 - 7.8

gastric pouch 3.27 + 0.87 2.6 ~- 5,1

silk (64 mesh/inch), diluting the retained

solid material to an appropriate volume (200

or 400 ml), and sampling using the method of

Clark et al. (1971) enabling calculation of

worm totals to a §.D. of = 5 worms. All nema-

todes in each sample were fixed in hot

alcohol, cleared in lactophenol, indentified and

counted,

An indication of the environment in each

region was obtained by measuring the pH of

the stomach contents of the first 20 wallabies

autopsied, using a glass electrode. The pH of

the stomach contents ranged from 7.8 in the

saccular region to 2.6 in the gastric pouch

(Table I). This agrees with the findings of

Moir et al. (1956) in some other macropods,

that the anterior 4/5 of the stomach appears

to be analogous to the rumen of the sheep

while the posterior 1/5 corresponds to the

abomasum.

Results

The nematode species studied were Cloacina

spp. (the genus considered as a whole because

some Of the species present have not been

described), Macropostrongylus pearsoni,

Qesophagonasies kartana, Rugopharynx

australis, and Labiostrengylus eugenii. L.

longispicularis Wood, whose distribution in the

stomach of the Red Kangaroo has been des-

eribed by Dudzinski & Mykytowyez (1965), is

present only in small numbers in the wallaby,

so was not considered in this study. Filarinema

sp., occasionally found in small numbers, was

restricted to the fourth region of the stomach,

and was the only species congregating in that

region,

Of the other species found each showed a

definite site preference along the length of the

stomach (Fig. 2). Cloacina spp, and M. pear-

soni were most common in the first section.

SITE SELECTION BY NEMATODES al

100

me}

§ 50

ra)

1 2

Stomach

M. pearsoni

O. kartana

L. eugenii

R. australis

Cloacina spp,

sites

Fig. 2. Histogram showing occurrence of different nematode species in the four stomach sections

referred to in text.

TABLE 2

Population structure of ZL, eugenii in four parts of

the wallaby stomach. Results expressed as % of total

number collected in each site, L — larva

% XL. eugenii

site 1 site 2 sie3 site 4

F ~ 2015 19.43 39.48 0

2 22.13 21.49 43.68 0

L, 53,51 45,82 16.50 0

Le 42 13.26 0.35 0

O. kartana is normally found in the oesophagus

and is present in the stomach only when there

is a heavy infestation,. R. australis was most

common in the third section of the stomach.

L. eugenii congregated in both first and

second sections of the stomach but most were

in the first. As with L. Jlongispicularis

(Dudzinski & Mykytowyez 1965) this may be

related to the position of the oesophageal

opening, worms being attracted to recently

ingested food. In wallabies with heavy infes-

tations, L. eugenii were seen protruding

through the sphincter into the oesophagus.

In newly opened stomachs L. eugenii was

found congregated in the paramucosal region

of the stomach lumen. The Cloacina spp. were

more often found in the central core whereas

O. kartana was frequently associated with the

crypts of the mucosal glands on the saccular

stomach wall. This suggests that a radial dis-

tribution, across the Ist and 2nd _ sections

separates these 3 species,

Seasonal observations on the occurrence of

M. pearsoni (Smales & Mawson 1978) suggest

that overlap with Cleacina spp. is minimal as

the former scems to be present in large num-

bers at times when those of the latter are low.

Nearly all the third and some of the fourth

stage larvae of ZL. eugenii were found in

nodules on the stomach wall in the second

section of the stomach, It was not practicable

to assess the number of worms in these lesions.

The site preference of L. eugenii was further

analysed in terms of population structure

(Table 2). No statistical difference was found

in the numbers of adults and larvae free in

sections 1 and 2, However, significantly more

adults than larvae were found in section 3.

Discussion

The environment along the digestive tract

is not stable, nor do changes occur abruptly,

‘$2 SITE SELECTION BY NEMATODRS

ruther one Tegion gradually merges with the

next. Consequently nematodes ure not restricted

to a single anatomical region but move within

limits to remain in the most favourable site

(Crompton 1973). When sections of the

wallaby stomach were ligatured no allowance

could be made for any environmental changes

in the stomach |umen which may have

occurred in an individual wallahy. Some of the

observed overlap between preferred sites may

have been due to the necessarily arhitrary

placing of the ligatures. Also when a large

number of the same species infest a host the

increased population density may cause some

of the worms to move to less favourable sites

(Crompton 1973), Examples of this appeated

to be the presence of O. kartana in the stamach

as Well as the oesophagus and M, péarsent and

Cloacing spp. In the second sections of the

stomach as well as the first.

Avoidance of the fourth section by those

species congregating in any of the three sections

comprising the saccular stomach was very

marked. No doubt the differences in digestive

function of the fourth section resulted in an

unsuitable environment. Similarly the nimen-

like conditions of the saccular stomach

appeared to be unsuitable for Filarinerma sp.

The nematode distribution described above,

showing considerable spatial separation of

niches both longitudmally and radially ts

similar to that found by Schad (1963) in

analyses of Tachygorietria spp. \n the colon of

the tortoise Testudo praeeu.

Where the site preferences of species overlap

spatially there are usually differences in food

habits, that is, behaviowral separation of niches.

Schad (1963) showed that While T. robusta

(Drasche) and 7 vtylova Thapar are found in

the same site oe species is an indiscriminate

fevder while the other selects fine particulate

matter, mamly bacteria, Observatlons of L.

eugenii suggest that it is an indiscriminate

feeder. Dudzinski & Mykytowyez (1965)

suggest that 4, longispicularis also feeds indis-

criminately. The differences in oral

morphology found amongst the Cleacine spp,

and M, pearsoni may be associated with

selection of different sized food particles. Some

species may feed on material ingested by the

host and others feed on'the bacterial or ciliate

populations present.

Petter (1966) suggested that the species

flock may vary with age and sex of host as well

as season. As only male wallabies were studied

the question of sex was not considered, Tt was

noted that Cloacina spp. were the earliest to

infest jocys but this was not investigated further

hecause of insufficient host numbers for each

range. Seasonal differences appeared to provide

niche diversification hetween M, pearsoni and

Cloacina spp.

The species present in the Cloacina spp.

flock have not been studied individually, but

general observations suggest that the species

composition of the flack does change with the

season.

Acknowledgements

Our thanks are due to Mr P, Davis who

collected the wailabies used in this study. The

work was supported by a Grant from the Rural

Credits Development Fund and » Common-

Wealth Postgraduate Research Awaril-

References

Cuasaub, A. G. (1956) Remareues sur les mema-

todes parasites du caecum des €éléphani«,

milieu cres présérve des phenomence de

selection. Cur. hehe. Seanc. Ace. Sci, Paris

243, 436-439.

Crark, C, §., Tuckem, A. M, & TorTos, FA.

(1971) Sarppling technique for estimating

round worm tordens of sheep pnd cattle,

Expl Purayvit. 30, 181-186.

Cromrron, D, W, T. (1973) The sites occupied

by sone patasie heliniths ja the allmen-

tary tract pf vertebrates. Biol, Rev, 48, 27-

Dupzmski, M. L. & Mykytowvez, BR. (1965)

Distribution of the nematode Fahiastrangylus

feovgispicularis (Wood) Wwilhin the stomach

of the red khangarog Megaleia rufa (Des

marest), Puravifalogy 55, 543-550,

CyripeivHs, M, & Barron, A. A. (1966) The

ontogeny of the stomach in the pouch young

of the red kangaroo. CSIRO Wildl. Res. 11:

THI-TRS,

Houmes, J. ©, (1973) Site selection by parasitic

helminths: Tnterspecific interactions. site

sceyeeation, und ther impurtanee to the

Uevelopment of helminth communities. Canes.

J, Zoal, 51, 333-347,

Mor, BR. J., Somers, M. W. & Wautno, PL (1956)

Studies in marsupial nutrition. 1, Ruminant-

like digestion in a herbivorous marsupial

(Seronix brachyares Quoy & Craimard |, Ast.

dy Rial, Sel 9, 293-301,

Myxyinwresz, Re (1964) A survey of dhe endo.

parasites of the ted kangaro Afeealom cele

(Desmarest). Parasitdory Sd, 677-693-

SITE SELECTION BY NEMATODES 83

Petter, A. J. (1963) Equilibre des especes dans

les populations de nematodes parasites du

colon des tortues terrestres. C.r. hebd. Seanc.

Acad. Sci. Paris 257, 2152-2154.

PeTTER, A. J. (1966) Equilibre des expeces dans

les populations de nematodes parasites du

colon des tortues terrestres. Mem. Mus.

wer Hist. nat., Paris, Serie A. Zool. 39,

-252.

Scuap, G. A. (1963) Niche diversification in a

parasitic species flock. Nature, Lond. 198,

404-406.

SMALES, R. L. & Mawson, P. M. (1978) Nema-

tode parasites of the Kangaroo Island Wal-

laby, Macropus eugenii (Desmarest). I.

Seasonal and geographical distribution. Trans.

R. Soc. S. Aust. 102(1), 9-15.

BATHYMETRY OF LAKE EYRE

BY J. A. T. BYTE, P. J. DILLON, J. C. VANDENBERG AND G. D. WILL

Summary

The bathymetry of Lake Eyre has been contoured from depth soundings obtained on six

expeditions, and one land tranverse of the dry lake. The lowest region of Lake Eyre North (the

lowest land area of the Australian continent) appears to lie in Belt Bay, and to have the elevation of

— 15.2 m A.H.D. The lowest region of Lake Eyre South (-13.2 m A.H.D.) occurs in the far

southwest. From the bathymetry, the surface area and volume of Lake Eyre as a function of water

level have also been calculated.

BATHYMETRY OF LAKE EYRE

by J. A. ‘T, Bya*, P. J. Dinton7, J. C. VANDENBERGt and G, D, WILLT

Summary

Hye, J. A. T., Ditton, BP, J,, YVawoenserc, J, C, & Wu, G. D. (1978) Bathymetry of Lake

Eyre. Vranas, R, See. §, dust, 102(4), 85-89, 31 May, 1978,

The bathymetry of Lake Eyre has been contoured from depth soundings obtained on six

expeditions, and one land truverse of the dry lake. The lowest region of Lake Eyre North

(the lowest land area of the Australian continent) appears to lic in Belt Bay, and to have

un elevation of

15.2 m A.\H.D, The lowest region of Luke Byre South (—13.2 m A.H.D.)

occurs in the far southwest. From the bathymetry, the surface area and volume of Lake

Eyre as a function of water level have also been calculated.

Introduction

The recent flooding of Lake Eyre has

supported a considerable water traffic, much

of which has been equipped for scientific

study, Of basic importance in this work is, of

course, navigation, which comprises position

finding and depth sounding. As a result,

approximately 387 soundings and some pre-

cision depth recorder traces have been ob-

tained at various periods between June 1974

and September 1976, These data enable the

bathymetry of Lake Eyre, which lies in the

lowest land basin of the Australian continent,

to be contoured, and the water storage of the

lake to be determined. Land levelling surveys

of the dry lake for Madigan Gulf (Bonython

1956) and Lake Eyre South (Bonython 1961)

Were also available for comparison with the

surveys of the flooded lake, [i was decided to

omit the results of the Madigan Gulf survey.

so that an estimation of any changes in bottom

profile due to the flooding would be apparent.

in Lake Eyre South, however, the number of

data points was very small and this survey

therefore has been included in the contouring.

Data sources

Data used in the construction of the bathy-

metry of Lake Eyre comprised soundings from

five shipborne expeditions, one helicopter sur-

vey, and one land traverse (Table 1). Apart

from the land ttaverse, all expeditions

occurred after the filling of Lake Eyre in

carly 1974,

TABLE |

Sources af bathymetric data,

Date t Expedition Method

Aug. 1960 — Bonython (1961) Levelling traverse

June 1974 — 9.2* E& WS (1976)+ Leadline soundings

trom helicopter

Leadline soundings

Soundings and preci-

sion depth recorder

Aug. 1974 — 9.2 EB & WS (1976)7

Aug. 1974 — 9.3* Bye (1976)

Dee 1974 — 98 E& WS (1976)+ Leadline soundings

Avg. 1975 —10.9 Clark (1976)** Leadline soundings

Sep! 1976 —i1.1) Clark (1976)** ~~ Leadline soundings

* Data in Lake Eyre South tive been corrected for dif-

ferences in level between Lake Eyre North and Lake

Eyre South,

| Lake Eyre data File, Water Resources Branch, Engin-

vering und Water Supply Dept, S. Aust,

Water level pn E & WS north gauge beard, Lake Eyre

North (m AWD).

** Lake Eyfe logbook of IBIS (unpubl.).

The first expedition (led by G.D.W.), in

which a helicopter chartered by the Engincer-

ing and Water Supply Department, South Aus-

tralia (E. & W.S,), carried out nine leadline

soundings at scattered points in both portions

of the lake, occurred in June 1974. Two

months later, a second BE. & W.S. expedition

(under the direction of the Chief Surveyor)

reached the mouth of the Cooper Creek by

boat, In the same month an expedition by the

Flinders University of South Australia (led

by J.A.T.B.), using a motor launch equipped

with a precision depth recorder, made a trip

hetween Curdimurka and the mouth of the

————

* School of Harth Sciences, Flinders University of South Australia, Bedford Park, S. Aust, 5042.

| Engineering and Water Supply Department, S. Aust.

J. A. T. BYE, P. J. DILLON, C. J. VANDENBERG & G. D, WILL

(AUG. 1960 )

BONY THON

E&WS

E 1974)

(JUNE

(AUG 1974)

FLINDERS UNIV

(DEC. 1974)

(AUG

E &WS

IBI

fo2)

—O-

|BIS (SEPT. 1976)

—1-

coe,

Pe COcoccDaG 7 IOQCOOSCADOOOEAS00

YV—Tang 9

and positions of individual soundings used as sources for bathymetric data in

Fig. 1, Cruise tracks,

Lake Eyre.

BATHYMETRY OF LAKE FYRE 87

Cooper Creck via Goyder Channel, Jn Decem-

ber 1974 the E, & W.S, party returned and

surveyed a large urea of Lake Eyre North as

far as the Warburton River to the north, and

Bandoo Hill to the west. Since 1974 the two

most significant charting expeditions have been

undertaken by Alvin and Max Atkinson and

Bob Clark of the Port Vincent Sailings Club,

in the “trailer-sailer” IBIS. The first expedi-

tion in August 1975, which wus planned by

J. A. Dulhunty of the University of Sydney.

comprised av leg from Level Post Bay to the

mouth of the Cooper Creek, followed by u

detailed east-west section, and a return lex via

Belt Bay. In September L976 the same crew

made soundings aver the southern half af Lake

Byte North and obtained a cood coveruge of

the lake bed in the vicinity of Bandoo Hill,

Belt Buy and Jackboot Bay, All the cruise

tracks (Fig. 1) were determined by triangula-

lion on landmarks (which are few) and dead

reekoning usually using a ships log.

In addition to the cruise programs, levelling

Iraverses in the Level Post Bay area between

Prescott Point and the easter shore of Lake

Eyre South, 6 km south of the Goyder Chan-

nel causewuy, were undertaken by the F. &

W.S. in August 1974 and September 1976.

The purpose of the levelling wis to establish

gauge boards in Level Post Bay and Goyder

Channel for the conversion of data on water

levels lo Australian Height Datum (A.H.D.).

The zero |. m) of the E. & W-S. north gauge

hoard near the entrance of Goyder Channel

m take Byre North was delermined co be a

height of —20.6 m A.H.D. The water level on

this gauge hoard at the time of each expedition

(Table 1), was used to reduce the bathymetric

data. Jn addition the zero of che level post in

Level Post Bay was found to be at —13,2 m

AH, This post wax erected by M, O,

Hughes of Muloorina Station in tune 1974,

close to the vite of the first level post in Level

Post Bay erected by C. W. Bonython in 1951

(Bonyithon 1955) and subsequently uprooted

hy floodwater in April 1974, The zero of

the first post (Known as the 100° arbitrary

reduced level) was assessed by Dulhunty ina

levelling survey in 1972 to be ~12.6 m A.H.D,.

(Will & Clark 1977)1.

In September 1976 a detailed survey of the

bathymetry of Goyder Channel was under-

raken, In general the depths obtained by

soundings are thought lo represent the lake

bottom oceurring at the base of the salt crust

whieh exists under dry lake conditions. The

trace oblained from the precision depth

recorder (Bye 1978) was a hard reflection

showing no fine strivture. The accuracy of an

individual depth measurement appears to

depend on three fuetors: (1) the measure-

ment technique: Gi) the effect of oscilla-

tions in waler level due to meteorological

causes, (it) the definition of the bottom. On

estimating error bounds of + G.10 m for each

of these factors an overall accuracy of atrout

+ 0.3 m is obtuined. The error bound (ii) is

an estimate for the Jake conditions under

which most of the hathymetne data were

obtained. Dulhunty (1976) hos assumed the

same bound for levels measured after a calm

period of not less than six hours, In addition

there are errors in position fixing. which in

must Cases are probably Jess than + 0.5 km

(Fook mean square absolute),

Rathy metry

The clevations. of the lake botlent from

eyeh expedition were plotted together an a

base map (1:250 000) from which the bathy-

metry was contoured in intervals of OS my,

except near the coastline (Fig. 2). tn yeneral

the agreement between the various cruises and

the traverses of the dry lake bottom was good,

althaugh the density of soundings (Tig 1) was

not sufficient to define features on a seale less

than | km. The Warburton and Kaluweerina

Grooves and a new feature, known as the

Cooper’ Depression (Dulbunty 1977), rudning

from the mouth of the Cooper Creck to the

north of Brooks Island, however, were

apparent from the data,

The deepest region of Lake Fyre is

apparently the eastern side of Belt Bay where

bottom levels of —15.2 A.H.D, ure found, In

this region therefore hes the lowest point on

the Austrulian continent. In| Madigan Gull

also there is a large deep region with cleva-

tion less than 15,0 m A.H.DA The bathy-

| Bstablishing A.H,D. at Lake Byre North and Jake Eyre South, Rept Surv. Be, Engineering & Water

Supply Dept, S. Aust.

“We are very grateful to Dr Dulbunty for providing detailed addiuonal soundiny legs in November

1976 in central eastern Madivan Cull. These results caused the authors to disallow same FE & W.S.

soundines in Madigan Gulf which suggested that » deeper depressian t- 15.6 m A.H.D,) existed

Nearer the eastern shore of Madigan Golf

88 J. A. T. BYE, P. J. DILLON, C. J. VANDENBERG & G. D. WILL

ad Poole + acts = =

i> ean \\WaARBURTON

\. \) River

> KALAWEERINA

CREEK

\ 2st

fo PN a

- oe \ Pn \

- 7 = \ SS

xO < \ COOPER

a \ CREEK

‘,

+ vA , ifs ‘

A \ 4 Pa 5 4

IBIS

ISLAND \ Y

__” c~ = {160

HUGHES), — va “3

par ws

Nh artemal Sh BRORE NAS \

DULHUNTY { Point aN 4 of

* Nis ISLAND J ] ) aN, NY

7 °

/ se NY

v / SAN

(~ “Sg \\

ae Abe SCO

(oa (BRS (Om

o~ BELT S| . \ “s

( Blo 3 \wat")

\ Bk

\y er

B\_.

Prescott

ere,

fi ed ‘a mm =

ar USS

4 + CURDIMURKA * 2 y

ed + + +

Fig, 2. Bathymetry of Lake Eyre. Contours in m A.H.D.

BATHYMETRY OF LAKE EYRE 89

TABLE 2

Surface area and volume, and elevation of Lake Eyre

Nerth and Lake Eyre South

Eleviar Surface Area Volume

tion tm North South Norih South

(A.H.D.) km2 km? 100m? 106m3

—15.0 310 _ 20 —

—14.5 960 _ 340 —_

—14.0 1.900 _— 1 660 —_—

—13.5 2810 —_ 2210 —

13.0 3.780 25 3.870 3

—125 4940 120 6 060 84

—12.0 6 080 290 8 800 135

—I15 6 860 570 12 000 345

—110 7520 B90 15 600 TLO

—1045 7920 1070 19 500 1210

—W.0 8 240 1170 23 500 1770

— 90 8 430 1 260 27 700 2 380

metry of Madigan Gulf is very similar to that

obtained in the land survey of Bonython in

1954 (Bonython 1956) indicating that there

has been no significant moulding of the bottom

by the floodwaters. The sill level between the

two portions of Lake Eyre in Goyder Channel

in September 1976 was —10.6 m A,A.D, This

figure is close to —10,1 m A,H.D, obtained

by Bonython in 1960 (Bonython 1961) indi-

cating that in Goyder Channel also the scour

produced by the floodwater was not large. The

deepest points of Madigan Gulf and Jackboot

Bay are respectively —15.1 m and ~ 15.0 m

A.H.D.

In Lake Eyre South there is the appearance

of a Jong depression offshore of the southern

coastline. The sill level (—10.6 m A.H.D.)

in Goyder Channel occurs about 8 km from

the entrance to Lake Eyre North,

Surface area and yolume versus elevation

From bathymetry the surface area and

volume of Lake Eyre North and Lake Eyre

South, as a function of water level, can be

determined by planimeter, The results (Table

2) indicate that the surface area of Lake Eyre

North and Lake Eyre South at the times of

the maximum levels in the recent flooding

were respectively 8.4 and 1.3 10%km*. The

maximum water depth anywhere in Lake Eyre

was 6.1 m (in Belt Bay in May—June 1974)

and the maximum volume of water was 32.5

Tl (in June-July 1974). The latter result is

very close to that of 32.0 TI obtained by

Bonython (1975)",

Conclusion

The bathymetry derived from ships’ obser-

vations has been found to be of sufficient

quality to reproduce the known features of

the dry lake basin, and to reveal some new

features. In addition the storage of Lake Eyre

North and Lake Eyre South have also been

calculated,

There appeared to be no significant mould-

ing of the lake bed by the floodwater by com-

parison with previous land levelling surveys.

References

Bonyruon, C. W. (1955) In Lake Eyre, South

Australia, The great flooding of 1949-50. The

report of the Lake Eyre Committee, R,

Geagr. Soc, Aust. (S.A. Branch) 27-36,

Bonytuon, ©. W, (1956) The salt of Lake Fyre,

Trans, R. Sac, S. Aust. 79, 66-92.

Bonyrnon, C. W. (1961) The uccurute deter

mination of the level of Luke Eyre. Proc. R.

Geoer, Soc. Aust, (S,A, Branch) 27-36,

Bye, J. A. T. (1978) Hydrological measurements

in Lake Eyre during 1974 and 1975, Cruise

Report, F.1.A.M.S. Flinders University of

South Australia. ;

Dutxunry, J. A. (1975) Shoreline shingle ter-

races and prehistoric fillings of Lake Eyre.

Trans, R. Sac, 8. Aust. 99, 183-188,

Duthunry, J, A, (1977) A bottom profile across

liake Eyre North, South Australia. J. Proc.

R. Soc. N.S.W. 110, 95-98.

8 Recording the event and spreading the information i Luke Eyre Newsletter, 2-3. Flinders University

of South Australia,

WATER BALANCE OF LAKE EYRE FOR THE FLOODED PERIOD

JANUARY 1974 —- JUNE 1976

BY G. TETZLAFF AND J. A. T. BYE

Summary

After the filling of Lake Eyre in early 1974 the volume of the water decreased from a maximum of

32.5 T1 in June-July 1974 to 16.5 Tl in June 1976. Study of the water balance equation indicates

that the major inflow of 38 Tl was from the Diamantina River system, and that local rainfalls and

the Cooper River system contributed 8 Tl and 2 Tl respectively. Loss by evaporation during the

period was 39.5 TI.

WATER BALANCE OF LAKE EYRE FOR THE FLOODED PERIOD

JANUARY 1974-JUNE 1976

by G, Tetzcarr* and J, A. T, Byey

Summary

Twrazcarr, G. & Bye, J. A. T. (1978) Water balance of Lake Eyre for the flooded period

January LO74-June 1976, Trans, RK. See, 8. Aust. 102(4), 91-96, 31 May, 1978.

After the filling of Lake Eyre in early 1974 the volume of water in the luke decreased

from a maximum of 32.5 Tl in June-July 1974 to 16,5 Thin June 1976, Study of the water

balance equation indicates that the major inflow of 38 T) was from the Diamantina River

system, and that local rainfalls and the Cooper River system coniributed 8 Tl and 2 TI

respectively. Loss by evaporation during the period was 39.5 TI.

Introduction

From early 1974, when the dry area of the

Lake Eyre busin was filled with water, a

general decrease in the surface area and the

water coutent of the lake has been observed,

Some remarkable deviations (rom the general

trend in water level have occurred, which

may be interpreted in terms of the various

inflows contributing to the existence of

the lake, The water balance of any luke is

dependent on only a few parameters, which

are related by the water balance equation,

AV —~ R ~ E+ 1, in which AV is the change

in volume of water (storage) in a lake, R the

precipitation on its surface, B the water loss by

evaporation, and T the net inflow including

surface and groundwater exchanges, For Lake

Eyre the net inflow may be replaced by the

inflow itself, because negligible outflow (sur-

face or groundwater) cat) be expected to occur

as the lake ties in Australia’s lowest basin,

several metres below mean sea level.

The inflow may be classified into three parts.

One: Jocal inflow mainly supplied by small

rivers und streams, but tncluding the Neuales

and Frome rivers, Two: the Diamantina

(including all northerly tributaries) and the

Cooper river systems, both of which have large

parts of their catchment areas situated in the

humid zones of inner Oucenslund. Three:

groundwater inflows inta the lake basin caused

ly the rising of the groundwater lable due lo

high rainfall rates. Thus, one can expect inflows

from river systems after high rainfalls in

Queensland, from Jocal streams after local pre-

cipitation, and from groundwater flows after

high widespread rainfalls producing seepage

over a large area of the Great Artesian Basin

surrounding the lake,

The AV-values for Lake Fyre are measured

indirectly by taking a series of surface levels

al o fixed position in each lake. A knowledge

of the bathymetry of the lakes allows the con-

version of the level recordings imto water

volumes (Bye et a/, 1978, Table 2), The read-

ing accuracy of an individual water level is

about “0,10 m, but fortunately most time

periods are well covered with measurements,

und hence the error on the adopted water level

curves (Fig. 1) is significantly smaller, The

cause of the scatter, apart from inaccuracies in

reading, is the effect of wind stress. Strong

wind conditions lasting for a long period are

however exceptional, and it is probable that

measurements not representalive of mean lake

levels can be recognised (e.g. the points with

very high levels in June and July 1974)., Errors

in converting walter level changes into changes

in Water volume are very small, because the

error On AV is proportional to the error on the

lake area at each depth. This is almost

certainly less than 1%; thus the error on a

typical AV of 1 Tl/month is only 0.01

T1/month.

“ Institut fiir Meteorologie und Klimatologie, Technische Universitat, Hannover, W. Germany.

+Sehool of Barth Sciences, Flinders University of South Australia, Bedford Park, S. Aust. 5042,

92 G, TETZLAFF & J, A. T, BYE

-80

bad

c=}

E LEVELS m(AHD.)

LAKE EYR

FMAM J

1974

JASON OD 3

FMAM

JASONODS FMAM 3

5 1976

* ELEVATION AT LEVEL POST BAY (LAKE EYRE NORTH)

c ELEVATION AT CURDIMURKA (LAKE EYRE SOUTH)

® WATER VOLUME OF LAKE EYRE NORTH

IN Tl

{nN Tl

Fig. 1. Lake Eyre levels and volume of water February 1974-October 1976.

During early 1974 a large flooding filled

Lake Eyre North and, from April onwards,

Lake Eyre South. The maximum height of the

water level of the northern basin occurred in

May-June 1974, and that of the southern in

September-October of the same year. The

maximum combined water volume (32.5 T1*)

occurred in June-July, After the peak of the

floodings had passed the losses exceeded the

still continuing inflows (June-October 1974),

Months of rapid decrease of the level followed

until February 1975, when local rainfalls

reduced the rate of loss, but with no sub-

sequent rainfall or inflows the level then fell

steadily until the late winter of 1975. The

channel between the northern and southern

basin closed about August 1975, and the levels

of the two parts of the lake afterwards changed

independently, In Lake Eyre South, the fall in

level continued unabated until by September

1976 only a few patches of water remained. In

Lake Eyre North however very high local rain-

falls (cf, Fig. 2) caused the level to remain

approximately constant between October 1975

and January 1976, and to rise temporarily in

February and March 1976. After this

interruption the level continued falling through

to September 1976,

The maximum surface area of Lake Eyre

North according to the bathymetric curye (Bye

et al. 1978) was about 8.5 10%km®? which gives

a mean water depth of 3.7 m (in June-July

1974) decreasing to about 2.0 m in September.

Monthly Precipitation Rates on the Surface

of Lake Eyre

Monthly precipitation rates for Lake Eyre

have been determined for the period January

1974-June 1976. The data which include all

rainfall observation stations maintained by the

Bureau of Meteorology in South Australia, and

some additional data from stations in the

Northern Territory, Queensland and New

+1 Tl = 10°m3

* Bureau of Meteorology, Aust. Rainfall Data, Monthly and Annual (unpublished).

WATER BALANCE OF LAKE EYRE 93

PRECIPITATION ON

mm month

3007,"

200F-

1ao0;-

LAKE

EYRE

JFMAMJJASONOYFMAMJJASONDJI FMAM

1o74

1975

1976

Fig. 2. Monthly precipitation on Lake Eyre January 1974-May 1976.

South Wales®, were displayed on maps for each

month from which the precipitation over Lake

Eyre was found by interpolation with an

estimated accuracy of + 10%. In general the

interpolated fields indicate a local maximum

over the lake, although low precipitation rates

sometimes exhibit a very irregular distribution

(Tetzlaff unpublished data).

The long term average monthly precipitation

in the Lake Eyre region has a well marked

maximum in February, and a maximum in late

winter (July-August): and the annual mean

precipitation is 120 mm/ year.

The rainfall during the times of the flooding

followed the usual annual cycle, only the

amplitude being enlarged (Fig. 2). In

February 1976 alone, twice the amount of the

long term annual mean value was found, In

1974 and 1975 annual rainfall exceeded all

previous observed figures, These rainfall

patterns during flooded years appear to be in

part attributable to feedback mechanisms Over

the lake which precipitate on average about

100 mm/ year (or 5% ) of the evaporated water

vapour (Tetzlaff unpublished data).

Evaporation from the Lake Surface

There are no direct measurements of

evaporation from the lake surface. Hence,

indirect methods must be applied to derive

estimates of evaporation, Of these the well

known micrometeorological methods (e.g. the

Dalton and Penman methods) are precluded

owing to a lack of systematic measurements of

characteristic parameters such as water tem-

perature, air temperature and relative humidity.

and hence use must be made of the water

balance equation itself. The difficulty is that of

the four parameters in this equation only the

precipitation rate R and the storage AV are

known. The inflow in addition to the evapora-

tion has to be regarded as unknown. It is

possible however from the precipitation data

for the catchment (mainly Queensland) and

locally, to find some periods during which any

inflow can be excluded. This occurred from

November 1974 to January 1975 and again

from April 1975 to July 1975, summer and

winter periods respectively, In this case

E = ~— AV, and inferred evaporation can be

compared with the measured pan evaporation

94 G. TETZLAFF & J. A. T. BYE

EVAPORATION

mm /month

300

200

100

OF LAKE

EYRE

TL/ month

2:5

JFMAMJJASONDJFMAMJJASONDJFMAM

1974

1975

19 76

Fig. 3. Evaporation from Lake Eyre January 1974-May1976.

values at land stations. Oodnadatta, Woomera

and Moomba all at about the same distance

from the lake were chosen, and an average pan

evaporation for the lake region was deter-

mined. The ratio between the inferred and the

average pan evaporation during the above two

periods was found to be a constant with the

value of 0.67, and the month by month

variation of the factor showed a low scatter,

suggesting an error bound on the constant of

+ 5%.

It is assumed therefore that this value may

be applied also to determine evaporation for

the remaining time intervals, and the resultant

monthly lake evaporation values are shown in

Fig. 3. The annual value is approximately

2000 mm. This figure is remarkably close to

the original determination of 1950 mm for

Lake Eyre for the year 1951 by Bonython

(1955), and is comparable to that for lakes in

similar climatic conditions such as Lake Chad

where an annual evaporation rate of 2250 mm

is observed.

Inflow into Lake Eyre

Detailed measurements of inflow into the

lake are’ generally not available and

inevitably strongly underestimated, as during

the recent floodings the waters often proceeded

on a broad front of several kilometres, of

which only a small part could be measured at

the gauging stations in the river beds of the

Diamantina and the Cooper rivers. The amount

of inflow of groundwaters is even more difficult

to obtain. This flow is very slow and rather

steady and can contribute noticeably only after

periods of several months (Holmes pers.

comm.). Therefore the total water supply to

the lake (inflow and rainfall) was determined

from the water balance by calculating

AV + E (Fig. 4). The negative values give an

insight into the accuracy of the deductions. The

errors are approximately = 0.15 T1/month.

This value corresponds to an error in the

estimated water level of the lake of only

+ 15 mm, which is significantly less than the

error for an individual water level measure-

ment.

WATER BALANCE OF LAKE EYRE 95

11 AZ month

INFLOW RATES

DEDUCED

P Theall. il :

JFMAMJJASONDJIFMAMJIJASOND JS FMAM

1974

1975 1976

Fig. 4. Inflow into Lake Eyre deduced from the water balance equation January 1974-May 1976.

The partition of the inflows into the con-

tributions from the Diamantina river system,

the Cooper river system, the local floods, and

the groundwater is an interesting problem, and

it could not be solved rigorously, though the

three surface components could be sufficiently

separated using information on the velocity of

advance of floods in the two river systems

(Bonython 1963). As a result it can be stated

that the Diamantina floods proceed generally

four times as fast as the Cooper floods. The

mean velocity for six floodings is 3.1 km/day

for the Cooper, and 12.5 km/day for the

Diamantina. In 1974 and 1976 the passage of

the floodings of the Cooper was observed at

Innamincka and Kopperamana. From _ these

96 G. TETZLAFF & J. A. T. BYE

data using the velocity of advance it follows

that the date of entrance of the Cooper flood

waters into the lake was not before the end of

April 1974, and not before July in 1976, By

April 1974 however the bulk of the water had

already entered the lake (Fig. 1). Hence, the

major contribution can come only from

the Diamantina river system, because ground-

water inflows are excluded at that stage.

In comparison with the first inflow rates, all

later inflow rates appear to be much smaller,

reaching about one fifth of the 1974 values in

1976, The 1976 floods contain not only con-

tributions from the river systems but also local

inflow from local rainfalls and possible ground-

water. During the period September 1974-

August 1975 no surface inflows are observed

except for those caused by local rainfalls. This

situation served for the determination of the

local inflows in relation to the local rainfalls.

The inflows originate from sourees such as the

Neales and Frome rivers. The increase in

volume of water at this time is that which falls

directly on the lake surface plus inflow. Using

the known precipitation rates it was found that

the local inflow contributes about the same

volume of water as does the rainfall. Adopting

this factor for the other periods we find that

the gain by local inflow is equal to the pre-

cipitation over the lake itself.

Total Water Budget

Applying the above conclusions for the

whole period of the flooding from 1974 to

June 1976 we obtain the total water budget

TABLE |}

Total water budget of Lake Eyre: January 1974-June

1976

Rainfall 8.0 TI

Local Inflow 8.0 TL

Infiow from Diamentina river system 38.0 TI

Inflow from Cooper river system 2.0 TI

$4.0 TI

Evaporation -39,5 Tl

BALANCE 16.5 Tl

(Table 1). It seems remarkable that the Coaper

Creek inflow was not of importance at any

stage in comparison with the northern flood-

ings, or indeed with the local water from pre-

cipitation. The evaporation is of such a

magnitude that with no more inflows from the

Diamantina river systems the lake is expected

to dry up in about one to two years (from

1276) mainly depending on the volume of

local rainfall.

Acknowledgements

The authors wish to express their

appreciation to all observers, In particular Mr

M. ©. Hughes of Muloorina Station, The

Engineering and Water Supply Department,

S. Aust., and Australian National Railways

Commission, who contributed the observations

of water level in Lake Eyre North and Lake

Eyre South shown in Figure 1. Many helpful

comments by Mr C. W. Bonython on the inter-

pretation of the data are also gratefully

acknowledged.

References

BonytHon, C. W. (1955) In Lake Eyre, South

Australia, The great flooding of 1949-50.

The report of the Lake Eyre Committee. R,

Geog. Soc. Aust. (S.A, Branch), 50-56.

BonytHon, C, W. (1963) Further light on river

floods reaching Lake Eyre Proc. R. Geogr,

Soc, Aust. (S.A. Branch) 64, 9-27,

Byer, J. A. T., Ditton, P. J.. Vanpengera, J.C,

& Wirz, G. D. (1978) Bathymetry of Lake

Eyre. Trans. R. Soe. S. Aust. 102(4), 25-88.

REDEFINITION OF THE AUSTRALIAN LEPTODACTYLID FROG

NEOBATRACHUS PICTUS PETERS

BY J. D. ROBERTS

Summary

Neobatrachus pictus is redescribed using morphological and male call data. The redescription is

based on topotypic material and an examination of syntypes. The geographic range is southern S.A.

and Victoria. Most published information about N. pictus is based on congeneric species. N. sudelli

(Lamb) is resurrected from the synonomy of N. pictus.

REDEFINITION OF THE AUSTRALIAN LEPTODACTYLID FROG

NEOBATRACHUS PICTUS PETERS

by J. D. Roperts*

Summary

Roserts, J. D. (1978) Redefinition of the Australian leptodactylid frog Neobatrachus pictus

Peters. Trans. R. Soc. 8. Aust. 102(4), 97-105, 31 May, 1978.

Neebatrachus pictus is redescribed using morphological and male call data, Phe redescrip-

lion is based on topotypic material and an examination of syntypes. The geographic range is

southern S.A. and Victoria, Most published information about N, pietas is based on con-

feneric species. N, sudelli (Lamb) is resulrected trom the synonomy of N. pictus.

Introduction

Most authors acknowledge that two species

of Neobatrachus (the type species N. pictus

Peters and N. centraliy (Parker))} occur in

eastern Australia (Littlejohn 1971; Cogger

1975; Barker & Grigg 1977), However, there

is considerable confusion about the identifica-

tion of individuals to each of these species.

For example Cogger (1975) figures the range

of N. pictus as only just extending into north-

etn Victoria. In contrast Brook (1975) indi-

cates that if is found in almost all of Victoria.

Similarly, Barker & Grigg (1977) figured the

range of N. pictus as extending only peri-

pherally into southeastern South Australia, so

excluding the type locality near Adelaide.

Despite Moore's (1961) doubts about the

validity of N. centralis Littlejohn (1965) pro-

vided clear evidence that al least two forms

of Neobatrachus occur in northwestern Vic-

toria, Littlejohn figured two audiospectro-

grams: one with a high pulse number, high

pulse repetition rate and low dominant fre-

quency was considered to represent N. cen-

tralis. The other had a low pulse number, low

pulse repetition rate and high dominant fre-

quency, and was referred to N, pictus. Here J

refer to it as “type B”. However, South Aus-

tralian frogs that I refer to N. pictus did not

make “type B” calls.

The identity of each of these species would

be clarified by examination of various data,

including male call, from type localities. The

type locality of N. pictus is near Adelaide,

and here I have attempted to redefine this

species, and so permit its geographic range to

be established,

The type locality

Parker (1940) and Moore (1961) state the

type locality of N. picrus to be “near Ade-

laide". Peters’ (1864) description was based

on material collected by R, Schomburgk of

Buchsfelde, “near Adelaide”. Buchsfelde is 4.5

km west of Gawler and is now known as Loos

(Praite & Tolley 1970).

Richard Schomburgk settled at Buchsfelde

in 1849 and lived there or in the Gawler area

until at least 1865 (Van Abbe 1960; Serle &

Ward 1976). Although there is nu direct evi-

dence, it is reasonable to infer that his cal-

lection was made at Buchsfelde, and that this

is the type locality of N. pictus.

Methods

(a) Material examined: Calls were analysed

from recordings made at seven sites! 7.5 km

N.W. of Gawler, ic, 5.5 km N, of Loos (14

frous),; 15.5 km N.W. of Penola (2 Progs);

Semaphore Park, 13 km N.W. of Adelaide

(t frog); Coffin Bay, 38 km W.N,W, of Port.

Lincoln (1 frog); 7.5 km 8S. of Kimba (1

frog); Roora Reservoir, Kimba (2. frogs);

Pilepudja Reservoir, 17 km N, of Kimha (2

frogs) and Muratchinu Dam, 33 km N. of

Kimba (1 frog), All recording sites ure in

* Department of Zoology, University of Adelaide. Present address: Deparimemt of Zoology, Univer-

sity of Western Australia, Nedlands, W.A. 6009.

9s J. D. ROBERTS

South Australia and all tape recorthings are in

my possession,

The following specimens were examined. All

wre wo the S.A. Museum; registration rmoe©-

hers refer to that collection. Cullection dates

ure provided only tor topotypes from 7,5 km

N.W. of Gawler, all collected by J, D, Roherts.

Tupotypic material: R16384 9, R16385-R16987 all

3d, all 2771.73; RIG3I8S GF Qiv.73: RiGIBy Y,

R16390-R16394 all cd, all 5.vi,73, Calls of eight

of these males were recorded. Other muterials

R2590 | $1 9 Lake Mamilton; R2776 4 9, Sel-

licks Heach; R2888 3 dot F 1, hetween Naime

& Bulhunnah; R3007 | ?, Kangaroo Islund; R3099

( 9, Muston, Kangaroo Island: R3474 1 9, Corny

Point: R348 2 3, Kangaroo Islund: R378R | of

1 2, Avenne Manges RA7L7 1 oY Reynellas RSU03-

5095 3) West Beach; R5096 | 2, West Beach;

RS5149 52), West Beach, R5175 | ff 1 2, Nara

coorte; R5176 | f, Pt Lincoln; RS195 220J, Cum-

mins; R5196 6), Hampstead; R5197 11, Hamp-

stead Gdns; RS497 1 9 Mr Graham. ar Mulicent;

R8355 UW, Hardwicke Bay; R&S356 11, Box War,

Lameroo; R&K44 1 4, Edeowie Gorge; R&YT4 21

9 JJ, Naracoorte: R8960 | 9. 16 km W) of

Vivonne Bay; R&Y63 L df 2 &, Lucindale: RS970

3.2 9, Naracoorte; R8977 UI, 96 kin N.NE.

of Frances: R&Y86 AC 3 9. Narmocourte: R997¢

| d, Hincks Nil Pk; RIOSST IT of 1 2, Narrung;

R12251 1 9 Sentuphore Pk; R13039 1 Z Nuri-

ootpa: RI3345 2 7 1, Mr Scott Nil Pk; R1356!

1 2 Minebool, nr Mt Gambier; RI3623 A-b 2

f 2 §, 1622.4 km S. of Naracoorte: RId256 |

4. tr Penola: RIS382 3929 11, Bangham Can-

servation Pk; RIS486 1 & Laura; RIGOL7 1 %,

Innes NU Pk: RIGH29 1 9, Sandy Ck Conservi-

tion Pk) R1I6308 7 of) Jip Jip Conservation Pk:

RI639S | ft 7.5 km WLW, of Gawler; R16396

1.9) bm S. of Kimba: R1A397-99 3 ¢ Roora

Reservoir, Kimbn; Rl64i0 1 4) Pilepudia Reser-

voir, 17 km N, of Kimba) R1l640}-2 2 4, 1545

km N.W. of Penola; R16403 7 429. 49.1 km N,

of Kingston: K16404 1 4 5.3 km N. of Peake

Risdos | of, 322 km S& of ME Mary; Rinadt

(41% Varna Sta, Eyre Peninsula; R1H4N7 1 fy

ato ka N. of KingMom KI6808 | P74 kon

SS.W_ of Coolutoa; RIAG09 1 2, 3.5 km S.W,

of Coolutoo, Rlpéi |) 48 kin NW, of Coola-

foo, RIGHT! 2 2 1 2 LG km SR. of Mr Batker

Riedi2 1 9 4.0 km WN. of Strathalbyn: RIGS

i, 28 km NON.W oof Littlehampton: RIG4i4 1

9, 26 kay W. of ML Barker: RIM4IS 7, 16-32

km S. of Kingstaun; RIGIIK 2 & | 2, Scorpion

Springs Conservation Pk; R647 | S 23.5 kin

N oof Menimagie; RIG4I8 2 of Whanmiidan:

RL6419 3 JAF. 24.5 km N, of Kinestuns RiGQa2

14 1 9. Lake Gilles Nit Pky RI6421 27, Mondy

Tunks, Wo of Ungaitin RIO? | S27 km SE.

of Kingston; Ri6d23 7 2) Banh Ri gaz vw

#+.6 km SSW, of Kybybolite: RIWd25 | 4) 0.6 kin

S.W. of Kybybolite; R16426 1 5, 0.3 haw NL of

Conjuum School, Comaum; R16427 | 9, 25 km

S.E af Glen Roy Rwy Stn} Klo428 7 of, 160

km N.W-. of Penolu; RIKG29 | DG 2.5 km S. of

Penola) RIMM LY LEB km SS uf Penula:

R643! (2, 4.7 km S, of Tarpeena; R16432 1

Allendale Bust, RI6433 1d 2 9, 26 km N.N-W-

of Nuracoorte; R1A434 7 ¢ 1 9, 28.4 km NNLW,

of Nuracoorte: Rif435 | 4 1 F, 5.4 km WN.E. of

Beachport; 16436 1 9. 21.7 km SE. of Rober

Ri6437 | 3. 5.2 km SSW, of Greenways; R1N438

2/19, 2.2 km NE. of Greenways; R16439 | &

(2 128 km NF of Greenways; RI6d40 7

7.4 km E.S.E- wf Kingston-

(bh) Call recording and analysis; Calls were

recorded of a Nagen UE NP, tape recorder

with Beyer M 100 microphone, a Uher 4400

Report stereo recorder with AKG, D 404 C

microphone, or a Sony TC-510-2 recorder

with ALK.G. D 190 microphone. th ull cases

tape speed was 19 cm/sec, Recording levels

Were set below —SdB ta minimise overload

distortion which could arise with signals of

short duration. All recorded frogs ‘were ecall-

ihg from sl] water, Waler lemperatures were

recorded at the calling site, but may slizhily

overestimate cloacal temperatures, For fifteen

froys where both data are available the mean

difference between water and cloacal tem-

peratiires was 0.16°C, This difference was sig-

nificant {Wilcoxon T 4.5, P <= .05). How-

ever. as only water temperature data wert

obtained jn some cases this problem cannot

be overcome,

Tape recordings were analysed hy playback

at half speed on the recorder used for field

recornling, With the oulput displayed on a

Tektronix 502 double beam oscilloseape and

photographed by a Grass C4 camera, A tite

marker (100 pulses/sec, derrved tram the 50

Hiv mains frequency) was displayed on the

second beam of the oscilloscupe, With half

specd playback the time marker Aleerively

represents S om sec, rather than the expected

!O m sec. intervals.

Only the list clear recorded call was ana-

lysed for cach Frog Successive calls of indi-

vidual lrogs were similar. Pulse repetition rate

was measured from pulses 7 to 10 and pulse

duration, dominant frequency and rise time

fie. the time from start in peak pulse armypli-

hide) were measured i pulses 7. & and & and

the three values averaged, Polses per call were

counted jn the last three recorded calls teither

from oscillograms or by playback at reduced

lape speed), and the three values averaged.

{e) fieogeaphie disteihatian aud biology: Diss

trisuuon daity were golluted jm three ways:

REDEFINITION OF NEOBATRACHUS PICTUS 99

if \ /

27.4 HAWKER~

o a _

LACRAMAN 5 J (@& 4

Ge<PORT LINCOLN a GAWLER R,MURRAY

aks pore

oS ADELAIDE

@ = Call analysed or call and specimen records

Fig. 1. Distribution of Neobatrachus pictus in S.A.

100

TABLE 1

Temperature effects on call compenent values,

Temperature range 8,5-22.0°C; sample size 14, Signifi-

cance of regression coefficients was compured with 0.

(ns. not significant, * p <.05, ** p <.01, *" p

<.001).

Inter-

Call Component Slope S.E. cept

Pulses/Sec. 1,188" O78 1.249

Pulse Rise Time — (1360+ 026 5.645

Pulse Duration ~~ 287 00 16.313

Dominant Frequency 0.011" 004 1,139

Mean Pulses/Call —O0473 ns. an 40.098

TABLE 2

Call camponent values and standard errars at 15°C for

temperainre dependent components. Sample mean atid

standard errar for pulses/ call.

Call Component Vulue 5B. Range _

Pulses / Seo. 1.0L 397 -

Pulse Rise Time (msec. ) 3.60 ALT =

Pulse Duration (msec.) 12,00 444 -

Dominant Frequency (kHz) 130.019

Meat Pulses/Call 33.07 1.323 23,7-43.4

from detailed analyses of field recorded calls;

by subjective evaluation of choruses heard in

the ficld (call records, Pig. 1), and by exa-

mination of specimens collected without call

data and held in the S.A. Museum (see p. —).

Observations. on general and particularly

breeding biology were made during field

recording trips.

(d) Morphology: 1 made a detailed examina-

tion of 11 specimens (9 od, 2 2, see Topoiypic

material listed above) collected 7.5 km N.W.

of Gawler, and the syntypes of N, pictus. The

following body dimensions were recorded:

snout-vent length; head length (from tip of

snout to posterior tip of jaw articulation);

a ee a ee ee ce ee ee ee ce ee eee Me

Fig. 2. Upper, oscillogram of complete cull of

male (R16393) recorded 7.5 km W,W.

of Gawler on 5.vi.1973. Lower, detail af

pulse simicture m pulses 7-8. In both

cuseés the lower trace is a lime marker

representing 5S msec, intervals, Call starts

on right.

J, D. ROBERTS

PULSES

wer

SECOND

/ 4 zh] 3 15 7 eo oat 240626 #3

WATER

Fig. 3, Geographic variation in pulse repctition

rate Values. Solid circles: Gawler; open

circles! Kimba area; open diamond: Pen-

Ola; open square: Semaphore Pk; solid

square: Coffin Bay, (See Material Exu-

mined for specific locality data.)

TEMPERATURE |)

head width (measured behind eyes between tips

of jaw articulation; eye length (horizontal dis-

tance from anterior comer of eye to anterior

edge of naris); tibla length (measured with

leg flexed so that bone fitted inside calipers).

Less detailed examinations were also made

of numerous frogs fram localities throughout

S.A.

Results

(a) Calls: Por the Gawler sample all call com-

ponent values were regressed on water tem-

perature; the results of this analysis are given

in Table 1. Only the average number of

pulses/call is not influenced by temperature.

Mean call component values (at 15°C, esti-

mated from the regression lines for tempera-

ture dependent vanables) are given in Table

2. A representative oscillogram is illustrated

in Figure 2.

The call of N. pietus can be characterised

by a high pulse number (33), low dominant

frequency (1.4 kHz) and a high pulse repeti-

tion rate relative to other Neobatrachus calls

known from South Australia (Roberts, unpub-

lished observations). Pulses are short (12

msec.) and have a smooth rise and decay

vycle (Fig. 2). Peak pulse amplitude rises

slowly for the first few pulses then evens out

(Fig. 2)-

Calls analysed from other sites in South

Australia closely resemble calls from Gawler,

and there is no evidence of significant gea-

graphic variation in any call components (Fig

3 illustrates this for pulse repetition rate).

The call Littlejahn (1965) considered to

represent N. cevtralis is similar to calls from

Gawler, and it is likely that in reality these

REDEFINITION OF NEVBATRACHUS PICTUS 101

individuals represent N. pictus. The identity

of frogs he referred to N. pictus is therefore

uncertain.

The calls described ybove are chiracterstic

of males calling strongly, At the Start of calling

sequences males sometimes make calls with

much lower pulse pumbers, However, such

calls have a pulse form, pulse repetition rate

and dominant frequency as detailed ahave-

(b) Geopraphie distelbution; The known rage

of this species in South Australia is given in

Figure 1. The speeies occurs throughout the

southern portion of the State, extending north

to Edeowie Gorge (40 km N.N_E. of Hawker,

S.A.M, R&S44), West to Yarna Station near

Lake Acraman, northern Eyre Peninsula

(S.A.M_ R1I6406) and east to the Victoria

horder-

Near Morgan and Blanchetown on the

River Murray, and north trom Kimbo on

Eyre Peninsula, N, pierus is replaced by un-

other species (possibly N. centralis) differing

in eall and morphology. Near Naracoorte and

Penola N. pictus occurs sympatrically with a

congener species Which can be distinguished

by male call but less reliably by morphology,

Calls of all these frogs ure the “type B" of

Litllejohn (1965),

J have no data on the distribution of N,

pictus outside South Australia, However.

Brook (1975) pave data on the distribution

of Neebatrachus in Victoria, partly derived

from field potebooks of Littlejohn and his co-

workers. If Brook adopted Lilllejoha’s call

nomenclature (see above), his records of "NV,

centralis" almost certainly refer to N, piceny.

This species therefore extends into western

Victoria, und in some sites is sympatric with

4 congenecric form.

The density of records on Figure | reflects

the intensity wf field investigaiton in variens

areas, and not necessarily the density of N-

picius. t have had little opportunity to work

in mid-northern South Australia but have spent

a considerable amount of time in the southeast

of the State,

(ct) Biolavy: N. pictus only breeds aller heavy

rain (usually more than 25 mm in 24 hr}

and probably breeds at any time of year. |

have observed breeding und calling activity in

Febriary, March and throughout winter and

eurly spring. Hreeding periods are shor! and

rarely last more thin uw few days. Breeding

ageresations are often dense, In July 1972,

near Kingston, 1 observed more than 150 frogs

man ares of ahout 225 my,

Males generally call While floating in Water

with the head above the surface but with the

rest. of the body submerged. Calling sites vary

fram exposed situations toa sites Where the

Male is Completely concealed inder flooded

vegetation, Mules often move when culling.

Occasionally they call from very shallow water

with only the ventral surface submerged,

Males ure not discriminating in their choice

of mates, and | have observed males trying to

amplex other males, spent females und even

muist rabbit dung on the pond margin. Am-

plectant pairs are quite often found on land

apparently heading For breeding pools. Am-

plexus is inguinal,

Breeding sites are Usually shallow. tem-

porary pools, though breeding may occur m

dams. | have never observed N-. pictus calling

or breeding in flowing water, The eggs are

Pigmented and deposited in large clumps or

in long strands several eggs wide. Initially the

eggs aye stick together with jelly, but ege

masses soon break down and fhe clearly en-

capsulated egys sink to the bottom of the

pond,

[L have no data on larval biology or mor-

phology though Martin (1965), ‘Tyler (1966)

and Watson & Martin (1973) all give illus+

trations of the mouthparts and sume other

detuls, However, Martin's (1965) and Wat

son & Martin's (1973) data are from speci-

mens outside the known range of N_ pictia,

and thus muy refer to some other, related

species.

Though N. plerus is cucountered most com-

monly when breeding, individuals ure oflen

welive on inoist evenings, and 1 have found

them on rouds und around swanips, and other

sites that may he used for breeding. This

species burrows and I have found individuals

buried hard against the underswle af large

stones, | have no dita on other burying sites.

{d) Aforphology: These data are presented as

4 redescription of N, pictys

Neobutrachus pictus Peters

Neubatrachuy pictus Pelers 1864 Monatsh. K,

Prevss, Akad. Wiss. Berlin 1864, 228,

Heleloporus pictis: Boulenger 1882 Car Barr

Sal. Brit. May, ed, 2, 272,

Definitions A Moderate to large species of

robust habitus. Limbs short, laree liner meta-

tarsal tubercle invariably with a black calling

edge. Dorsal skin, particularly en the antenor

half of body, covered with numerous, fine

102 J, D. ROBERTS

TABLE 3

Proportions of 11 N. pictus from near Gawler.

Ratio Mean Range

Head width; Head length 1.22 1.16-1,35

Eye/ Eye-naris 1.55 1.33-1.82

Eye-naris/Internarial span 1,00 0.83-—1,14

Head length/Snout—vent length 0.35 0.33-0.39

Tibia length/Snout-vent length 0.34 0,.25-0.38

Fig, 4. Neohutrachus pictus, Comaum, S.A.

small warts which are spinose in breeding

males, Distinguished from related species

either by its large size, distinctive call or, lack

of a skin connection from the knee across the

groin to the side of the body.

Description: Head high, wider than long and

roughly one third of snout-vent length (Table

3). Snout rounded when viewed from above

and angled slightly posteriorly in profile. Nares

dorsal and, when viewed from above, closer

to end of snout than to eye. Internarial span

greater or less than eye to naris distance

(Table 3). Canthus rostralis slightly rounded.

Eye large and prominent, its diameter about

one and one half times eye to naris length

(Table 3), Pupil a vertical slit; iris covered

with fine dark veins on, in life, a golden back-

ground (Fig. 4). Tympanum not visible ex-

ternally but present and roughly circular.

Vomerine teeth divided medially; their pos-

terior margin in line with posterior margin of

choanae. Vomerine teeth in close contact

medially, or slightly divided and may be in a

straight series or with lateral ends angled

slightly fowards snout. Tongue ovoid to cir-

cular; covers most of floor of the mouth,

Attached closely anteriorly but posterior and

lateral margins free.

Fingers short and cylindrical. No inter-

digital webbing; all fingers fringed, the fourth

least (Fig. Sa), Dark brown to black nuptial

pads well developed on first and second fingers

of breeding males, extending from base of

each finger to at least ultimate joint. Pads ex-

tend underneath base of first finger (Fig. 5a)

but only occur on medial side, and medial

upper half of second. In some specimens there

is fine extension of pad past ultimate joint on

both fingers. Dark, finely spinose material of

nuptial pad may be Jost in preserved speci-

mens and underlying, calloused area is difficult

to distinguish, Finger lengths usually 3 > 1 >

2 > 4; rarely 1 = 2. Subarticular tubercles

well developed and irregular number of inter-

digital tubercles. Tubercles at base of second

and third fingers often divided. Generally two

large, flat palmar tubercles: that at base of first

finger more prominent. Nuptial pad may over-

Fig. 5. a. Right hand of male (R16393); b. Right foot of male (R16391); c. Right foot of female

(R16389); d, Groin of N. pietus (R16393); e. Groin of male making “type B” calls from

8 km W. of Blanchetown (R16449). In d. and e, arrow indicates area of difference, In a.

b, and c, the bar represents 5 mm.

REDEFINITION OF NEOBATRACHUS PICTUS 103

fap medial edge of inner palmar tubercle (Fix.

5a),

Hind limbs short with thia averaging one

Third oF snout-vent length (Table 3), Toes

short and cylindrical with order of Jengths

4>5 > 5 >2 > 1. On one foot of R16399

toc 5 > 3. Subarticular tubercles poorly deve-

loped and may not be obvious on fifth toe, No

Wuter metatarsal tubercle but large, shovel

shaped, inner Metatarsal tubercle, usually

edged with black or rarely light brown.

Blackened section wlways much longer than

maxinium Width and symmetric about mid

tine (Fig. 5b, ¢). In males, webbing between

tues extensive, extending to or beyond ultimate

joint, with distinctive almost rectangular inden-

tation between third and fourth, and fourth

lind fifth toes (Fig. Sb). At tip of fifth toc

Webbing may appear almust as fringe. In

females webbing much less extensive, reaching

only to second joint on fourth toc, and deeply

indented between all joes (Fig, 5c).

Ventral surface, top of foot, femur and

underside of arm smooth, Dorsal surface, head

and eyelals, upper side of anns, tibia and

underside of foot usually bear numerous, fine,

smooth warts. On posterior half of dofsum

warts may only occur in band down mid-fine,

Tr breeding males nutnernus smull, short, sharp

black spines. Cloacal region bears fine white

ariunules, Just above jaw (extending back lo

aliave vem) there may be roughly linear series

of linge white granules, occasionally fusing to

form fairly distinct stnpe,

Ventral surface white; mandibular margins

or Whole chit may be Tightly suffused with

grey or light brown, In preservative dorsal sur-

face varies from sight to dark grey with

humerous small to medium darker spots, Edges

ol spots usually diffuse. There may be «a

narrow, While lo cream md-dersal stripe, often

interrupted. OF the eleven specimens trom

near Crawler, three hid no stripe, three a clear

stnpe uni five an inlerrupled siripe. In life,

havkgroimd colewr is venerally a yellowish

green with spots dark brown to black,

The eleven speeimens fran pear Gawler had

an averave snout-Vent length of 45.7 mm

(40,5-S52.0 vant,

Geographic vartalion Vrogs from all paris of

the range int SAL vary only tn the following

fespects: it series of tales Fron and near

Kimbu the for webbing is much fess extensive,

and closer ty that in feniiles fom Gawler

(Pig. Sc, In males from Penal the webbing

fs more cxtensive but through southeastem

S.A. males have more extensive webbing than

females. Some of this variation may be sca-

sonal as reported for N. pelobatoides (Parker

19-40).

In some specimens, particularly from the

Mt Barker-Balhannah area of the Mt Lofty

Ranges, as well as a mid-dorsal stripe there

was an clongate V-shaped mart extending pos-

teriorly trom above the arm with the point of

the V in line with the eye, In yu few frogs from

southeastern S.A. and the Mt Lofty Ranges

the tip of the first toe bears a light brown to

hlack spot.

The maximum snout-Vvent lengths recorded

were 62.6 nm {(d R16416, Scorpion Springs

Conservation Pk) and 60.7 mm (¢ RLO857,

Narrung),

Call> Relatively long, averaging 33 pulses (19

pulses/sec. at water temperature of 159°C),

Dominant frequency |,3 kH¢.

Comparivon with other species: The call of N-

pictus clearly distinguishes it (rom congeners

known from 8. Other Neobatrachus encoun-

tered all had similar calls with higher domin-

unt Frequencies (from 1,5-L,7 kHz), low

pulse numbers (average about 15) and at any

given temperature a much lower pulse repeti-

tion rate than N. pietus; my “type B" call of

Littlejohn (1965).

Adults of these other call types are cither

much smalicr (average S—V 36 mm) with

large. clearly demarcated spots on the dorsal

surface (southeastern $A.) of are light brown

or goldeti coloured with skin extending from

the side of the body across the groin to the

knee (Fig. 5e) (northern, northeastern and

northwestern $.A.). In N. pictus skin only ex-

tends marginally along the upper leg from the

side of the body (Fig. Sd), The skin enclosed

groin ulso occurs in the small form jn seuth-

eastern S.A., but is not a constant feature of

these Iroys.

Type speciniens

There are five syntypes in the Zoologisches

Museum, Humboldt University! 9507, a sub-

adult ¢? female) of 31.3 mm, and a juvenile ?

Notuden ertelaneseaphus,; 4725 a partly de-

composed adult female of 45,0 mm and a

poorly preserved male of 41.8 mm: 4726 a

well preserved gravid female of 55,1 mm S-V

and 56.4 mm (total length measured to pos-

terior extremity of body beyond the vent. It

is clear from the size and other details that

Peters based his description on No. 4726. It

104

werees with the original and this description

in size and all other pertinent respects.

Discussion

The distribution data in Figure 1 combined

with Brook’s data for western Victoria pro-

ably represent ihe total range of this species.

As N, pictus is replaced to the west, north-

west, north and northeast in S.A. and to the

east in Victoria (Brook 1975} by “call type

B" frogs, the only possible extension is into

southern and eastern N.S.W. Harker & Grego!

recorded “type B” calls 24 km §&. of Condob-

lin, N.S.W., attributing them to NV, pictus. LE

their use of (he name N-. picruy is consistent

throughout the range they wive for this species

(central N.S.W. as far as Queensland and

south into Victoria) then there is little chance

that N. picius (sensu stricto) octurs anywhere

in N_S.W. of Queensland,

Previous redescriptions of N. pictus (Parker

1940; Moore 1961) ditfer from mine in

several details. However, he character most

profitably used in distinguishing N. pietes from

Neohatrachus making “ype B" calls (extent

of skin in the groin: Fig, 5d, &), was not con-

sidered by either author. The differences be-

tween my description and thuse of these

authors may reflect the fact that in all proba-

bility none of the specimens examined by

them are conspecilic with N. pictus. Parker

examined material from Melbourne and Sand-

hurst (= Bendigo, Keed 1973) in Victoria,

Urana and Ryalstone in N.S.W, and a skeleton

from "Australia". Moore's description seems

to be largely based on specimens collected at

Mt Stromlo, A.C.T, Uo omy interpretation of

the range of N, pictus is correct, none of these

sites fall within the range of this species.

The distribution data T have presented show

¢learly that N. pieruy occurs on the Eyre

Peninsula, Muin, Lee & Littlejohn (1958),

Cogger (1975) and Barker & Grigg (1977)

have failed to recognise this Fact. Furthermore

this species fs not yet known to occur in

N.S.W., aud published ranges extending across

J. D. ROBERTS

NSW. and into Queensland (Cogger 1975;

Barker & Grigg 1977) are likely to be in error,

Heleioporus sudelli Lamb (1911) Fram

Warwick, Queensland has been considered a

synonym of N. picrus (Hosmer 1948, Moore

1961) though Parker (1940) — expressed

doubts. Because 1 have established that N.

pictus does not occur in Queensland, this

synonumy cannot be sustailted, Thus I resur-

rect N. sudelli (Lamb) as a valid species, and

possibly a senior synonym of N_ centralis

(Parker),

The relationships of N. pictus lo congeners

is unclear’, Parker (1940) argued that N. pelo-

hatoldes is the western analogue of N. pictiis,

and that these two species are closely related:

a sentiment reiterated by Main, Lee & Little

john (1958) and by Littlejohn (1967), How-

ever, as Parker's concept of N, pictus is now

suspect the real relationships are more

obscure, This problem will only be resolved

following a thorough te-cxamination of

material from all over Australia, variously

referred to ceniralix, pictus and sudelli, The

status of Neobatrachus populations making

“type B” calls in S.A., N-S.W. and Victoria

should be included in such a review,

Acknowledgments

During most of this research J held » Com-

monwealth Post Graduate Research Award.

Research finds were also supplied by Murray

Park College of Advanced Education. The late

Michael Smyth assisted with field recording.

Bev Roberts measured many of the call ascil-

lograms. Philippa Horton translated Peters’

description und Mr B, Stankewytsch-Janusch

prepared Figure 4, Dr T. F. Honston allowed

access to material in the SA, Museum, and

syntypes Were loaned by Dr Peters, Zoolo-

gisches Museum, Humboldt University, Berlin.

Mike Tyler offered advice and encouragement

and critically read the manuseript.

To the above and to the numerous persons

who: either sent specimens or recordings my

sincere thanks,

References

Banker, J. & Gaia, G, (1977) “A field guide to

Australian frogs.” (Rigby: Adelaide.)

Brook. A.J, (1975) The distribution of Anuran

amwonlidaas In Victoria, Vier, Mat, 92, 104-

Cnacea, HG. (1975) “Reptiles and amphibians

of Australia.” (Reed: Sydney.)

Hosmer. W. (1958) A note on the identity of

Heleioperes sudelli Lamb, N, Qld Nat. (120),

“ter

1 Cassette recording of mule mating calls of 44 species of southeastern Australian frogs. J. Darker &

G. Grigg. Zoology Building, University of Sydoey.

REDEFINITION OF NEQBATRACHUS PICTUS 105

Lams, J. (1911) Description of three new batra-

chians from southern Queensland. Ann. Qld

Mus. 10, 26-28.

LirrLEsOHN, M. J. (1965) Vocal communication

in frogs. Aust. Nat. Hist. 15, 52-55.

LITTLEJOHN, M. J. (1967) Patterns of zoogeo-

graphy and speciation in south-eastern Aus-

tralian amphibia. Jn A. H. Weatherley (Ed.),

“Australian inland waters and their fauna.”

(Australian National University Press: Can-

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LitTLEJOHN, M. J, (1971) Amphibians. Jn “Vic-

torian Year Book No. 85.” (Commonwealth

Bureau of Census and Statistics: Melbourne.)

Main, A. R., Lee, A. K. & LITTLEJOHN, M. J.

(1958) Evolution in three genera of Aus-

tralian frogs. Evolution 12, 224-233.

Martin, A. A, (1965) Tadpoles of the Melbourne

area. Vict. Nat. 8, 139-149.

Moore, J, A. (1961) The frogs of eastern New

South Wales. Bull. Am. Mus. nat, Hist. 121,

149-386,

Parker, H. W. (1940) The Australian frogs of

the family Leptodactylidae. Novit. Zool. 42,

1-106.

Perers, W. (1864) Ubersicht de von Hrn.

Richard Schomburgk an das Zoologische

Museum eingesandten Amphibien, aus Buchs-

felde bei Adelaide in Siidaustralien. Monatsh.

K, Preuss. Akad. Wiss. Berlin 1863, 228-236.

PRAITE, R, & ToLLey, J. C. (1970) “Place names

of South Australia.” (Rigby: Adelaide.)

REED, A. W. (1973) “Place names of Australia.”

(Reed: Sydney.)

Serce, G. & Warp, R. (1976) (section eds)

Volume 6, R-Z. Jn B. Nairn (general Ed.),

“Australian Dictionary of Biography.” (Mel-

bourne University Press: Melbourne.)

TyLer, M. J. (1966) “Frogs of South Australia.”

(South Australian Museum: Adelaide.)

Van ABBE, D. (1960) The Germans in South

Australia. Aust. Letters 3, 26-34,

Watson, G. F. & Martin, A. A. (1973) Life his-

tory, larval morphology and relationships of

Australian Leptodactylid frogs. Trans. R.

Soc. S. Aust. 97, 33-45.

SALT TRANSFERS BETWEEN NORTH AND SOUTH LAKE EYRE

BY J, A. DULHUNTY

Summary

Investigations in 1977 indicated that approximately 30° tonnes, or 7.4% of the salt crusts in Lake

Eyre North were transferred to Lake Eyre South by overflow of saline floodwater through the

Goyder Channel during the major 1974 flooding. Absence of salt crust in the south lake prior to

1974 and evidence of three greater prehistoric floodings, indicate return of salt to the north lake,

between high-level floodings, by a process believed to be solution in rain water and transport in

underground water towards the lowest area of the salina.

SALT TRANSFERS BETWEEN NORTH AND SOUTH LAKE RYRE

by J. A. DULHUNTY*

(with a calculation of the rate of groundwater movement, by J. W, HoLMes)

Summary

DOLHUNTY, J. A, (1978) Salt transters between North and South Lake Eyre. Vranas, KR. Sine

5. Aust, 102(4), 107-112, 31 May, 1978.

Iivesiigauions in 1977 indicated that approximately 30" tonnes, or 7.4% of the salt crusts

in Luke Eyre North were transferred to Lake Eyre South by overfluw of saline floodwater

through the Goyder Channel during the major 1974 flooding. Absence of salt crust in the

south lake prior to 1974 and evidence of three greater prehistoric floodings, indicate return

of sali to the north lake, between high-level floodings, by a process believed to be solution in

rain water and transport in underground water towards the lowest area of the salina.

lutroduction

Luke Eyre is a large normally dry salina.

consisting of two parts—Lake Eyre North and

Lake Eyre South, commonly referred to as the

nerth und south Jakes, connected by the

Goyder Channel (see Fig. | and Bonython

1955), The lake forms the sump of a large

internal drainage basin (Wopfner & Twidale

1967). When rivers rising in high rainfall

areas reach Lake Eyre, they flow into the north

lake to produce minor flooding of part of its

bed, or less frequently major flooding over the

whale of its bed (Dulhunty 1977; Bonython

& Mason 1953), The south lake normally

receives only small quantities of water from a

relatively small arid drainage area on the

soulhwestern side of the internal drainage

hasin, producing only minor flooding, On rare

occasions, possibly once in several hundred

years (Dulhunty, J. A. 1975) the north lake

floods to a high level and overflows through

the Goyder Channel into the south lake,

The purposes of this paper are (i) to record

an estimate of the quantity of salt transferred

to the south lake during the 1974 major flood-

ing, and the nature and distribution of result-

ing new salt crusts in the south take, and (ii)

io consider transfers by prehistoric floodings

and natural processes of return of salt to the

north lake.

Salt crust distribution

The bed of the north lake slopes gently from

north co south, and that of the south lake from

northeast to southwest, Hard crystalline salt

crusts up to 64 cm thick (Bonython 156;

Duthunty 1974) occur in the southern bays

of the north lake, which are the lowest areas

of the lake as a whole, where final evaporation

of floodwaters and brines takes place. Smull

quantities of Jocal rain water accumulate in

the south lake, and evaporate or soak into the

bed, but no hard crystalline salt crusts had

been reported or known to occur prior to the

1974 flooding of Lake Eyre. Bonython (1961)

described the bed of the south lake in 1960

as encrusted with soft powdery salt forming a

layer “never thicker than a fraction of an

inch”, but no solid salt crust like that found

in Madigan Gulf. In 1939 the present author

walked over part of the bed and found con-

ditions similar to those described by Bonython,

Water levels in North and South Lake Eyre

The bed of the Goyder Channel rises to

sill] which is about 2.0 m above the general

level of the adjacent north lake shoreline, and

the shoreline at the lower southwestern end of

the south lake. The sill is also about 44 m

above the deepest parts of the north lake, and

3.4 m above the deepest parts of the south

luke (see Fig. 1),

The A.H.D. values of the spot heights

shown in Figure 1 for the south lake, ure based

on original levelling by Bonython and Fenner

in 1960 (Bonython 1961), Their heights were

recalculated to A,H.D. values of hench marks

* Depariment of Geology and Geophysics, University of Sydney, Sydney, N.S.W. 2006,

108 J. A, DULHUNTY

¥ MADIGAN 14 4

1°}

v7 --

—/2-4 @ SPOT HEIGHT

ON BOTTOM, METR

BENEATH SALT WD.

\-/3-5~ BOTTOM CONTOUR

va GENERAL DIRECTION OF

SHOLLOW SUBSURFOCE

WATER MOVEMENT.

Fig. 1. Lake Eyre South and southern bays of Lake Eyre North showing relative bed levels and regional

groundwater movement.

along the Alice Springs Railway near Curdi-

murka, recently amended by Mr R. T. Smith

for Commonwealth Railways and adjusted to

the A.H.D. value of Bench Mark L 40/6440

(Dept Lands, S. Aust.) at Prescott Point,

adopted by the Engineering and Water Supply

Department, Adelaide (Will & Clark!) as

established A.H.D. value for the Lake Eyre

area. A.H.D. values for Lake Eyre North,

shown in Figure 1, are based on levelling by

the author in 1972 as yet incomplete and un-

published.

The only occasion on which a definite over-

flow, from one lake to the other through the

Goyder Channel, was authentically observed

and recorded was during the 1974 flooding to

the greatest depth ever recorded, and possibly

for some 500 years (Dulhunty, J. A. 1975).

The flooding commenced in February 1974,

Water in the north lake rose to the level of

the sill and commenced flowing through the

Goyder Channel on about the 19th March

1974, Flow increased until May of that year

when a maximum mean lake level of about

9.1m A.H.D. was reached, approximately

1.0 m above the original sill level. It then

decreased slowly as the north lake level fell

and the south lake level rose, until an equili-

brium level between the two obtained in

October 1974, Small amounts of water then

Will, G. D. & Clark, J. (1977) Establishing A.H-D. at Lake Eyre North and Lake Eyre South.

Report, Sur. B., Engineering and Water Supply Dept. Adelaide

SALT TRANSFERS BETWEEN NORTH AND SOUTH LAKE EYRE 109

LAKE EYRE

Pa - r

( yet 7

) yiede- Ni

/ - q

GOYDER CHANNEL

TO LARE.EYRE NORTH

7 LEGEND

~~ S_-)SOPACH ON SALT CRUST/om)

Cc J TRAVERSE LINE FRUM SHORE

Fig. 2. Lake Eyre South showing salt crust distribution and thickness in October 1977.

moved back and forth through the channel

with changes in wind direction, until water

connection ceased during August 1975.

Transfer of salt during 1974 flooding

Water flowed freely through the Goyder

Channel for seven months, during which time

its salinity varied from 10 to 50 g/l The

volume of water which flowed through the

channel cannot be calculated accurately as rate

of flow varied widely, and the water required

to fill the south lake came from local rain in

iis catchment area as well as from the north

lake. However, it was evident that a great

quantity of salt had been transferred from the

north to the south Jake in aqueous solution

during the period of overflow.

After water ceased to flow into the south

lake, and it dried up in 1977, large areas of

its bed were covered with a hard white crys-

talline salt crust for the first time on record,

The crust closely resembled that which had

occurred over the southern bays of the north

lake before the 1974 flooding. Practically all

the salt formations and types of crust pre-

viously observed in the north lake (Bonython

1956; Dulhunty, R, 1975) were seen in the

south lake in varying degrees of development

in 1977. The only significant difference was

greater porosity and lower bulk density in the

south lake crust, due probably to immaturity

and a» somewhat more open texture in which

additional salt had not yet crystallised, Also,

in some places, lateral spaces or voids, from

0.5 to 3 em wide, filled with water and occa-

sional transverse salt crystals occurred on hori-

zontal planes within the crust. All salt crust

thicknesses recorded in this paper and in

Figure 2, are nett figures excluding lateral

spaces.

Quantity of salt transferred

A survey wus carried out of salt crust thick-

ness and distribution in Lake Eyre South in

October 1977. Results are shown in Figure 2..

Traverses were run out from the shore along

9 lines, A to H and J, across the lake bed

(Fig, 2), Nett crust thicknesses were deter-

mined at intervals of 200-500 m depending

on rate of change in thickness. Isopachs were

then drawn through points on the traverse

lines, and interpolated across intervening arens

using all available information and indications

obtained by aerial and surface reconnaissance.

110

The resulting isopach map (Fig, 2) is believed

jo be a good general overall pictuve of the

eecurrence of salt crust in the south lake tn

Octoher 1977.

The area of thickest crust, occurring within

the 20 cm isopach, varied up to 24 cm in the

vicinity of the lowest place in the south lake

discovered near Emerog Point in 1960 by

Bonython (1961), A maximum thickness of

29 em was measured at one place near the

shore off the northern tip of Em¢roo Point, i

a channel Washed out by Walter flowing round

the point.

Bonython (1956) recorded the mean bulk

density for salt in Lake Byre North as about

1.49 tonnes per m*, und calculated the total

salt content, above the surface of the true lake

bed to be about 408" tonnes. Determinations

of bulk density of the immature salt crust in

the south lake, gave a mean value of about |

tonne for m*, representing about 67% of the

bulk density of the older north lake crust.

The quantity of salt crust in Lake Eyre

South, in October 1977, occurring above the

surface of the true lake bed, calculated from

isopach values, enclosed areas and a hulk den

sity of 1.0 tonne per m', was about 30%

tonnes. This indicales that approximately

7.4% of the salt crust ut Lake Eyre North

was transported to Lake Evre South during

the 1974 flooding.

Prehistoric floodings and sali transfers

The study of wave-built shingle terraces

tlong the shores of the north lake {DuThunty,

J. A. 1975) established at least Uhree pre.

historic floodings to depths of 0.7, 1,6 and 2.8

mm) greater than in 1974, al intervals of the

order of 500, 1500 and 3000 years before

present. Quantities of salt equal to, if not

greal¢er thin that carried through the Goyder

Channel in 1974-75 must have beet) trans-

ferred to the south lake by cach of the pre-

historic flooditygs, yet no sall crust was known

in the south lake, prior to the 1974 flooding,

for at leust 40 years. This means thar in some

way salt must he returned to the north lake

helween cach of the maior floodings which

carry it into the south lake.

Return of salt to Lake Kiyre North

There would seem to be only three ways it

which salt could be returned to the north lake,

|. Wind wunrport. Transport of salt as an

airhorme powdery efflorescence, of absorbed

on dust particles (Bonython (956; Grabag

1920), by prevailing southwest to southeast

J, A, DULHUNTY

winds from the crust in the south luke to the

forth lake or its catehment, is theoretically

possible ond probaly bas happened ta some

stall extent. Lt wouwd require solution of hard

salt crust in partly saturated rising water, and

rapid drying at the surface to form a powdery

sult, or film absorbed on dust particles, which

gould become airbome. In both forth and

south lakes crusts salt solutions have been

seen rising along cracks and drying at the sur-

face to form soft cellular, or lace-like salt

masses almost efforescent bul not powdery.

The salt masses did oor seem ta he eroded hy

wind to become airborne, even in strong winds,

hut remained until dissolved in rain water,

from which the sali was added to hard crust

by recrystallization on evaporation. Nor was

evidence seen of dust being welted with salt

solution and drying to become airborne,

Although no direct evidence of wind traits

porl of salt was seen at Lake Eyre, it could

have operated as a minor contributing factor

in return of salt to the north lake.

2. Solution in surface floodwater, The most

direct and simplest way in which salt could he

teturned to the north lake would be by solution

m surface floodwater filling the south lake

ind overflowing into the north lake. However,

no authentic report, record or observation

cxisis of Lake Evre South filling independently

of the north lake, and overflowing to the north

(Bonython 1969), Nor docs it seem likely that

this couldl have happened under present con-

ditions of aridity (Bonython 1960), which

must have existed for at last 3000 years in

the relatively small drainage area of the south

lake. The circumstances in which the worth

lake filled in both the 1949-50 and 1974 flood.

ings, indicate that a fare high ramfall Years

when the south Inke could have filled, the

north Inke Would fuve filled first and over-

flowed into the seath lake, preventing effective

transfer of salt to the north. So return of salt

to the north lake by serth-lowiny floodwaters

would seem to have been so wnlikely that it

must be discounted,

The possibility of water, from minor fillings

in the south lake, being blown by south

westerly wind up across is hed and through

the Goyder Channel, must also be discounted.

During the 1949-50 floadings inean take level

rosé to Within 24 em. of the sill level

(Henython 1966) bit noe water was knewn fo

be blown south throngh the channel Also,

after the 1974 flooding, when water receded

in the south lake to a little south of the south.

SALT TRANSFERS BETWEEN NORTH AND SOUTH LAKE EYRE ii

ern end of the channel, at some 40 em below

the sill, no water was known to have been

blown north through the channel, Even if filled

to the general level of its northern shore, al

aboot J10 m AH,D, (see Fig, 1) water

would have ta have been blown up through a

vertical interval ef L.O m to Bow north through

the Goyder Channel, which would seem im-

possible,

3. Solurion in subsurface grourtedwater,

Limited quantities of rain water, from an aver-

age annual ramlall over the south lake of

Jess than 125 mm and brief flows. of river

water from its arid catchment area, accumu-

late at times, perhaps once every two or three

vears, in relatively small areas of its lake bed.

After dissolving salt, some of the water could

pass down through the bed and merge with

shallow groundwater moving generally to the

north beneath country separating the north

und somth Jakes (Pig. t). Such regional move-

ment of groundwater could certainly be ex-

pected from the higher country south of the

railway, north beneath the south Jake towards

the lower parts of Lake Eyre North (see Fig.

1),

The difference between lake bed levels in

the south lake and the southern parts of the

north Jake 1s illustrated in Figure 1, It shows

the battom contour of © 13,5 m AVH.D, equi-

valent to the lowest point im the south Jake,

close to the shorelines round Madigan Gulf

and Jackboot and Belt Bays, Practically the

whole of the lake bed in the three bays is up

to LAlom below the lowest point in the south

lake, and Up to 3,5 m below other parts of its

bed, This difference in elevation over the wide

area of the three hays would promote a posi-

tive Movement of groundwater to the north.

It would be most active during and following

years of higher rainfall, During years of very

low rainfall it may well be interrupted by

insuflicient intake to maintain continuity of

Water and flaw,

The groundwater carrying salt from Lake

Fyre South would eventually surface in Magi-

gan Gulf and Jackboot and Beli Bays, where

the base of the salt crust is at, or slightly

below the level of the “dry lake” watertable.

Tt would then move up through the crust to

evaporate and deposit its salt content at the

surface, This is believed to be the principal

factor contributing 10 the return to the north

of salt periodically dissolved in floodwater and

carried by overflow to the south lake.

Acknowledgments

It is wished to acknowledge (i) valuable

assistance of Muloorina Station including the

station aircraft in aerial reconnaissance over

Lake Fyre South piloted in 1976 by Mr M, O.

(Blue) Hughes and in 1977 by Mr Malcolm

Mitchell who also helped in running ground

vontrol traverse line H (Fig, 1) in country

of difficult access, (ij) helpful discussion with

Mr Warren Bonython, and with Messrs G_ D.

Will and J. Clark of the Engineering and

Water Supply Dept, Adelaide, and (iii)

research facilities of the University of Sydney

awd funding by the Australian Research Grants

Committee.

References

Bonyrunan, C. Wo & Mason, B, (1953) The filling

and deving of Lake Eyre, Geogr. J. 119(3),

321-330,

BonyTHon, C, W., (1955) In “Lake Eyre, South

Australia. The Great Flooding of 1949-50,"

The report of the Luke Eyre Commitee. R.

geogt. Soc, Aust. (S, Aust, Branch), pp. 7-9,

27-37. (Grilli) Press: Adelaide, )

Bonytnon. ©. W. 11956) The salt of Lake Eyre

—its occurrence in Madigun Gulf ane its

possible origit. Trans. Ri Soc. 8, Aust 79,

66.92.

Bowron, C, Wo (1960) A decade of watching

for water in Lake Eyre, Prac, R. geaer. Sac.

Ait. OS, Auer. Arancl| G1, 2-8.

BonyTHen, C, W. C1961) The accurate deter.

mination of the level of Lake Eyre, dhid, 2,

AT7-43.

Duitiunry, 1. A. (1974) Salt crust thickness and

lake bed conditions in southern areas of Lake

Eyre North. Trans. R. Sec. S. Ausi, 98(3),

125-133,

Duvyunty, J, AL (1975) Shoreline shingle ter-

races and prehistoric fillings of Lake Eyre,

thid, 9904), 183-188.

Ducnunry, J. A. (1977) The arid terminal role

and evolution of Lake Eyre in Australis,

Proc. Intemat Conf,, Arid Terminal Lakes.

Webber State College, Ogden, Utah. In press.

Dutnunty, &. (1975) “The Spell of Luke Eyre”,

pp, 16-19. (Lowden: Kilmore.)

Cruanau, A. W. (1920) “Principles af Salt Depo

sitton,” 1st Edm. (MeGraw-Hill: New York.)

Worrpner, H. & Twipare, C. R. (1867) In 0. N,

Jennings & J. A. Mabbutt (Eds). “landform

Studies from Australia and New Guinea") pp

118-143, (ALN_LU, Press: Canberes,)

112 J. A. DULHUNTY

CALCULATION OF RATE OF GROUNDWATER MOVEMENT FROM

LAKE EYRE SOUTH TO LAKE EYRE NORTH (by J. W. Holmes)

Suppose the geometry of the lakes can be

simplified to the diagram in Figure 3.

Lake Eyre a 7

rh eo ao

pe .)

~— -

26km—————+}

The rate of groundwater flow is given by

-# Ad

Q KA At ’

Where K is the hydraulic conductivity that we

will assume to be 1 m day, A is the cross-

sectional area through which the aquifer fluid

flows (= 2 % 105 m*), and Ag/Al is the

hydraulic head gradient (= 5 * 10).

Therefore

Q=1 * 365 * 2 ¥ 108 * 5 & 10% m§ yr

= 4 X% 10% m' yr,

The amount of salt to be transferred is 30

% 10° tonnes. Suppose it is transported in a

solution of about 100 g F! concentration. That

is, a solution volume fiow would be required

of about 3 % 10% m*, The time required for

this transfer would be about 7.5 * 10° years,

consistent with Dr Dulhunty’s statement that

the filling of Lake Eyre South by overflow

from Lake Eyre North may happen at a recur-

rence interval of ~1000's of years.

The physical transfer of the same salt as is

infiltrated through the bed of Lake Eyre

South to the bed of Lake Eyre North would

take a longer time. The aquifer volume can

be estimated to be 20 km * 20 km & 100 m,

and if the aquifer porosity is approximately

0.3 then the volume of fluid is about 1.2 %

10 m*. One pore volume would be replaced

by an annual flow of 4 X 10¢ m® yr in 3 ¥

10° years on the average. The salt solution

having its origin in Lake Eyre South would pro-

bably not emerge into Lake Eyre North earlier

than about + million years after it was en-

trained into the bottom of the south lake.

If these order-of-magnitude calculations

give a correct guide to the general picture of

the hydrology of Lake Eyre South relative to

Lake Eyre North, they suggest that there may

well be zones of lesser and zones of greater

salt concentrations in the aquifer fluid moving

so slowly towards Lake Eyre North. Such

zones would be expected to occur in response

to variations in local climatic conditions. The

gradients for flow are assumed to be relatively

stable and appropriate to the present land

levels. The mild tectonic activity of this region

could entirely invalidate any time-scale predic-

tions that go beyond about 10° years,

Dr Dulhunty states that the maximum depth

of water in Lake Eyre South occurred in early

1975 and that water connection across the sill

was severed in August 1975, The level of the

sill appears to be 9.1 m. He states that Lake

Eyre South dried up in 1977, That is, the

maximum depth of +13.5 — 91 = 44 m,

dried up in two years. This implies an evapora-

tion rate of 2200 mm yr+, and is in good

agreement with our understanding of net

radiation into the interior of Australia and the

energy available for evaporation of water from

a large lake,

MACROPICOLA OCYDROMIN.G. N.S.P. (NEMATODA:

STRONGYLIDAE) FROM A WESTERN AUSTRALIAN KANGAROO

BY PATRICIA M. MAWSON

Summary

The new genus is placed in the family Strongylidae, sub-family Globocephalinae, because of the

large subglobular buccal capsule, without leaf crown, cutting plates, or anterior teeth, with regid

mouth opening, and with three large oesophagal teeth. It differs from Globocephalus in the number

of teeth, form of teeth, form of the dorsal ray, and position of the vulva.

MACROPICOLA OCYDROMI N.G. NSP, (NEMATODA: STRONGYLIDAE)

FROM A WESTERN AUSTRALIAN KANGAROO

by Patricia M, MAWson*

Summary

Mawson, P.M, (1978) Macropicola ecydromi n.g.. n.sp. (Nematoda: Strongylidae) from a

Western Australian kangaroo. Trans KR, Soe, S. Aust. 102(4), 113-115, 31 May 1978,

The new genus is placed in the family Strongylidue, sub-fumily Globocephalinue, because

of the large subglobular buccal capsule, without leaf crown, cutting plates, or anterior

leeth, with regid mouth opening, and with three large oesophageal teeth. It differs from

Globoceplalus in the number of teeth, form of the dorsal ray, and position of the vulva,

Introduction

The new species and genus described in this

paper is one of the only two strongylid nema-

todes to be found in Australian marsupials.

The first, now under description. was also from

a macropod,

The genus Hypodoniuy MGnnig, 1929, pre-

viously considered a — strongylid = (sf.

Uncinariinae), was discussed by Inglis (1968)

who referred it to the Amidostomatidac, This

genus is at present under revision (Beveridge.

in preparation).

Holotype male and allotype female of Mac-

ropicola ocydromi will be deposited in the

South Australian Muscum, Other material is in

the Australian National Helminth Collection,

in the South Australian Museum.

All worms were fixed in hot formalin, and

cleared for light microscope examination in

lactophenol. Specimens for use in the S.E.M,

were brought through ethanol to xylol, and

coated first with carbon, and then gold-

palladium.

Macropicola n.g.

Strongylidae: Globocephalinae: Anterior

end with flattened cuticular cap surrounding

hexagonal mouth opening and bearing amphids

and submedian papillae. Buccal capsule large,

subglobular, with dorsal groove, and with three

solid = multi-tuberculate oesophageal teeth.

OesOphagus clubshaped, Male: bursa entire,

not deeply lobed, ventral rays together, ventra-

laterals separate from = postero and medio-

laterals, externo-dorsal from dorsal ray, dorsal

ray bifurcate each branch dividing again; spi-

cules long, alate; gubermaculum present.

Female: tail short, conical; vulva close to anus,

ovejectors parallel, uteri pro-delphous. Para-

sites of the large intestine of macropod marsu-

pials. Type species: Macropiceola ocydromi

n. sp,

This genus has been placed in the family

Strongylidae rather than the Trichonematidae

because of the subglobular shape of the well-

developed buccal capsule, IL has been referred

to the subfamily Globocephalinae because of

the absence of Jeaf crown, teeth or cutting

plates around the mouth. Of genera in this

group, Macropicola most closely resembles

Globoacephalus Molin (1861), differing from

it in the number of final branches of the dorsal

ray, the number of oesophageal teeth, and the

more posterior position of the vulva, Globo-

cephalus marsupialis Freitas & Lent (1930)

was described from a South American mar-

supial, Metachiropy opossum.

The only other strongylid from Australian

marsupials is the new genus being described by

Dr J. Beveridge. This differs markedly from

Macropicola in the presence of two well

developed leaf crowns,

Macropicola ocydromi n.g., sp.

FIGS 1-9

and localities: Macropuy /uliginesus

ocydromus Gould, from near Albany (9 9,

Host

” Department of Zoology, University of Adelaide, North Tce, Adelaide, S. Aust, 5000,

114 PATRICIA M. MAWSON

Macropicola ocydromi: Figs 1-3: Head. In lateral, en face, and dorsal views, respectively, to same

scale. Fig. 4: Oesophageal region. Figs 5-6: Bursa in lateral and dorsal views. Fig. 7: Genital

cone, dorsal view. Fig. 8: Posterior end of female.

4 3, from 1 host), Jandacot Experimental

Stn, W.A. (5 2 from one host), and near

Perth (29, 1 do, from one host).

Males 12.8-13.6 mm long, females 18.3—20.4

mm, tapering only slightly anteriorly and pos-

teriorly. Cephalic cuticle forms thick flattened

plate, slightly wider than succeeding body, and

bears four small conical submedian papillae,

two amphids, and a central anteriorly directed

octagonal mouth opening. Buccal capsule

longer than wide and widest at its midlength

(Figs 1, 2). Dorsal wall of capsule thicker in

its basal quarter length, where it is penetrated

by the duct of dorsal oesophageal gland; after

its emergence through wall the duct connects

with encircling groove, cut into capsule,

following a course as shown in Figs. 1 and 2.

From each of the three sections of oesophagus

a stout tooth projects into buccal cavity, each

tooth provided with a number of short pointed

° * bs

Macropicola ocydromi: Fig. 9: Head cut longi-

tudinally to show inside of buccal capsule.

MACROPICOLA OCYDROMI 115

projections (Figs 1, 2, 3, 9). Oesophagus

1400-1500 »m in male, 1600-1800 pm in

female, cylindrical anteriorly widening pos-

teriorly. Nerve ring 690-750 ym from head in

male, 700-770 ym in female. Small conical

cervical papillae and excretory pore shortly

behind nerve ring (Fig. 4).

Male: Bursa entire, longer dorsally. Arrange-

ment of rays shown in Figs 5 and 6. Postero-

lateral ray with branch from its base, passing

dorsally. Genital cone (Fig. 7) large, posterior

lip of cloaca with three pairs short projections.

Spicules 990-1000 ym long, giving a ratio of

spicule : body length of 12.8-13.6.

Female: Body tapers suddenly in region of

vagina to short conical tail, 130-190 »m long.

Vulva 220-300 »m from tip of tail, vagina

short, ovejectors parallel, prodelphous. Egg in

uterus (none in vagina) 150 x 70 pm.

The specimens described in this paper were

collected by N. Allen, and were sent to me by

Dr G. de Chaneet of the Animal Health

Laboratory, Department of Agriculture,

Western Australia. I am very grateful to have

received this material. The photomicrographs

were taken by E.T.E.C. Autoscan in the Cen-

tral Electron Optical Laboratory of the Univer-

sity of Adelaide. I am indebted to Dr Karl Bar-

tusek of this laboratory for help in taking the

micrographs and to P. G. Kempster for

developing and printing them.

References

Freitas, J. F. T. & Lent, H. (1936) Estudo sobre

o genero Globocephalus Molin, 1861 (Nema-

toda: Strongyloidea). Mems Inst. Oswaldo

Cruz 31, 69-80.

IncLis, W. G. (1968) The geographical and evo-

lutionary relationships of Australian tricho-

strongylid parasites and their hosts. J. Linn,

Sac. (Zool) 47, 327-347.

Moun, R. (1861) Il sottordine degli acrofalli

ordinato scientificamente secondo i resulta-

minti delle in dagini anatomiche ed embrio-

geniche. Mem. R. Ist. veneto Sci. 9, 427-633.

Monnic, H. O. (1929) Hypodontus macrapi, a

hookworm of the kangaroo. Annu. Rep. Dir.

Vet. Serv. Pretoria 15, 307-309.

VOL. 102, PARTS 5 & 6 31 AUGUST, 1978

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Grubb, E. A. A. Stratigraphy, palynology and implications of organic bands in a

small quaternary basin, near Palmer, South Australia - - 117

Sheard, M. J. Geological history of the Mount Gambier Volcanic Complex,

southeast South Australia - - - - - - = 125:

Daly, S., Webb, A. W. & Whitehead, S. G. Archaean to early Proterozoic banded

iron formations in the Tarcoola region, South Australia - - 141

Tyler, M. J., Davies, M. & Martin, A. A. A new species of hylid frog from the

Northern Territory - - - - - - - 151

Van Deur, W. J. Earthflows in the Yankalilla area of South Australia: significance

of rainfall, soil properties and Man’s activities - - - - 159

Hails, J. R. & Gostin, V. A. Stranded shingle beach ridges, upper Spencer Gulf,

South Australia: evidence for high wave energy dissipation

during the late Pleistocene — - - - - - - - 169

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STRATIGRAPHY, PALYNOLOGY AND IMPLICATIONS OF ORGANIC

BANDS IN A SMALL QUATERNARY BASIN, NEAR PALMER, SOUTH

AUSTRALIA

BY ELIZABETH A. A. GRUBB

Summary

The strtigraphy and pollen content of dominantly sandy sediments in a creek bed near Palmer have

been examined. Organic bands appear to reflect the presence of permanent standing water in a

settling pond from about 8000 years B.P. to some time more recent than 6600 B.P. The generic

content of the vegetation then was comparable to the present, but the presence of spores of

Anthocerolates suggests that the climate was slightly wetter.

STRATIGRAPHY, PALYNOLOGY AND IMPLICATIONS OF ORGANIC BANDS

IN A SMALL QUATERNARY BASIN, NEAR PALMER, SOUTH AUSTRALIA}

by EuizAbetu A. A. GRuBBt

Summary

Gruss, K. A. A. (1978) Stratigraphy, palynology and implications of organic bands in a

small quaternary basin, near Palmer, South Australia. Trans. RK. Soc. S. Aust. 102(5),

117-123, 30 August, 1978.

The stratigraphy and pollen content of dominantly sandy sediments in a creek bed

near Palmer bave been examined, Organic bands appear to reflect the presence of permanent

standing water in a settling pond from ubout 8000 years B.P. to some time more recent

than 6600 B.P, The generic content of the vegetation then Was comparable to the present,

bul the presence Of spores of Anthocerotales suggests that the climate was slightly wetter,

Introduction

Ah intermittently flowing stream 11) km

south of Palmer, South Australia, has deeply

incised earlier deposits, exposing organic layers

in its steep banks. The site is interesting be-

cause it is the only known Holocene site con-

taining organic sediments in the Mt Lofty

Ranges. It is critically positioned hear the

eastern limits of the Ranges, in a boundary

zone between the woodland and open forest

vegetation characteristic of the higher and

wetter ranges to the west and the scrub and

mallee, common on the Murray Plains in the

east,

This paper describes the stratigraphy and

gives pollen counts from the organic sedi-

ments, und discusses the implications of these

results in the light of work done on material

ol comparable age from other parts of

southern Australia.

Gorge Creek, lat. 34°55'S, long. 139° 108,

flows in a shallow valley running east from Mt

Beevor towards the Murray Plains (Fig. 1).

Mt Beevor is 480 m high, and is a spur of the

higher and wetter Mt Lofty Ranges. Above the

site, which is at an altitude of 200 m, the

ereck drains an areca approximately 8 km long

and ut the most 3 km wide. Below the site the

Valley 1s constricted by rocky outcrops und

the creck runs to the Murray Plains 3 km away

through a narrow pass between the hills, which

form the eastern-most edge of the Mt Lofty

Ranges,

The mean annual rainfall 1s estimated as

about 400 mm, Daily mean maximum tem-

peratures at nearby Murray Bridge range from

28.9°C in February to 15,8°C in July, and

daily mean minima from 15.1°C (February)

to 5.5°C (July). It is likely that similar tem-

peratures are experienced at the site, modified

a little by the constricted valley formation of

the surrounding hills which probably tend to

trap cold air, Prevailing winds are from the

west and southwest.

Stratigraphy

A stratigraphic section (Fig. 2) was deter-

mined from nutural exposures in the steep-

banked gully of Gorge Creek. The deposit is

about 100 m long; its breadth is uncertain but

appears to be about 15 m. Alternating bands

of sand and organic matter are about nine m

thick (Fig. 3). The lower and more richly

organic bands form discrete layers, but the

upper bands ure less rich und less distinct, Up-

stream and downstream there is a uniform

brown sand which fills the bulk of the valley

floor, Schist of the Kanmantoo group lies only

a few centimetres below the present stream

* §4 Thornton Way, Girton, Cambridgeshire CB3 ONJ, England.

+ This paper is based on: Grubb, BE. A. A, (1967) Analysis of a semi-fossil organic deposit near

Palmer. South Australia, M.Sc. thesis, Department of Botany, University of Adelaide (unpublished).

11K ELIZABETH A. A. GRUBB

135"05'

4a%le

Achelosctn

a9euc!

Fin, 1. Topography of upper reaches of Gorge Creek, showing position of deposit (arrowed), Palmer

is 11 km to the north,

bed along the whole length of the deposit, and

there is a particularly notable outcrop near the

downstream end. It seems most likely that the

deposit began to accumulate in a small water-

hole or swamp retained behind a barrier

formed by the schist. However, the deposit

now extends over the schist barrier. Subsequent

incision by Gorge Creck has formed # narrow,

steep-banked gully, exposing the layers shown

in Fig. 3.

The sands are of varying colour and texture,

ranging from white through various shades of

yellow, orange and brown to black organic

sands and through fine and coarse sand to

gravel (Fig, 2), Very little clay is present. The

organic layers range from the black sand to a

heavy moist peattike material. There is no

evidence of charcoal, The richest organic

layers have been numbered one to seven (Fig.

2), und examined for the presence of pollen.

Two radio carbon dates were obtained. The

oldest organic layer (7) was dated at 6600 +

100 years B.P. A date of 8000 years was ob-

tained for a more recent layer, and this makes

it difficult to say with certainty when the

earliest sedimentation occurred,

Methods

Samples were collected from each organic

layer. As the layers were exposed sands were

simply sampled using 2.5 x 5 cm glass vials,

Slabs of the peat-like layers approximately 20

x 20 cm, were removed and transported in

plastic bags; in the laboratory fresh surfaces

were exposed and subsampled for analysis.

Subsamples of 1 g were processed using

standard techniques given by Faegri & Iversen

(1950), The most satisfactory means of pre-

paration was treatment with 5% potassium

hydroxide for 15 min., followed by acetolysis

and vibration using a ‘vibraflute’ (Tshudy

1960). The dehydrated residues were mounted

in glycerine jelly and stained with safranin.

A reference collection was made of the pol-

len grains of about 200 species commonly

found in the Palmer area now. Spores proved

to be common in the deposit and this neces-

sitated a small collection of fern and bryophyte

spores as there was at that time no suitable

reference text for these species in Australia.

Vegetation of the study area

Specht (1972) has mapped the probable

pre-settlement vegetation of the Palmer area

STRATIGRAPHY, PALYNOLOGY AND ORGANIC BANDS

us ‘woodland to open-forest with herbaceous

understorey’ dominated by Eucalyptus camal-

dulensiy (mainly in the valley bottoms), £&.

odorata and Casuarina stricta, The area was

opened up for European settlement about 1850

und has been extensively cleared to leave an

open grassland with occasional scattered trees.

Within 2 km of the site can be found Banksia

marginata, Callitris collumellaris, C. preissli,

Casuarina stricta, Execalypius anceps, £,

camaldulensis, E. fasciculosa and E, porose.

In most of the area the conimonest trees are

eucalypts, but on the rocky slopes surrounding

the study site Casuarina stricta is relatively

more prominent. The mallee eucalypts (E.

anceps and LE. perasa) occur in diserete out-

liers on sandy or rocky soils.

Native shrubs and sub-shrubs have heen

largely eaten out but some species may be

found still: Acacia spp., Billardiera serica-

phora, Buryaria spinasa, Correa schleehtan-

deli, Dodonaea viscosa, HMaloragiy hetere-

phyla, Melaleuca neglecta, Olearia sp., Pime-

lea strictum. Rhagodia nutans, and several

small legumes. Three ferns found commonly

ure Cheilanthes tenuifolia, Pleurosoruy ruti-

faliuy and Preridium esxeulentum,

Within | km of the deposit are pools con-

luining Potamogelon crispus and Ruppia mari

tina, and in the areas surrounding them grow

Carex tereticaulis, Juncus sp., Lepidasperme

laterale, Leptocarpuy brownii, Machaerine

juncea, Scirpus amevicanus and S. nodasxuy, In

other areas probably seasonally waterlogged

ean be found Cypertis gymnecaylos and

Juneus spp,

Nomenclature follows Black (1943-57)

except where revised by Eichler (1965).

The pollen record and its evaluation

Layer 1, an organte sand, and layer 2, an

organic layer whose stratigraphic origins are

obscure, yielded no pollen. Layers 3, 5, 6 und

7 contained pollen in meagre quantities, the

average slide having a count of about LOO

pollen grains. Layer 4 uppeared as richly

organic as these four, but the average pollen

count was only | or 2 grains per slide, and it

was decided to ignore iL. However, it was quite

rich in diatom skeletons and a small circular

scale, possibly also of diatom origin (7ATelo-

sira, David Thomas, pers. comm.).

The pollen counts obtained are given in

Tables | and 2. Beeause of difficulties ex-

perienced in trying to concentrate the pollen,

T have included in Table J total counts of all

Iya

valley floor

"jj white sand

ws -— yellow sand

ae =" orange sand

7 brown sand

—— 2

-="_ gravel

‘ mums Ofganic matter

=aom clay

——

= —

=. 21 mottling

me 5

5 ais

os 6

minis 7

——— water level

Disgrammatic representation of sediments

in deposit, showing organic coloured sunds

al top, mottled white sands in middle and

organic bands containing pollen near base.

Layers sampled for pollen analysis are

numbered (and their thicknesses indicated

helow in parentheses): 1, very sandy. no

pollen: 2, richly organic, but stratigraphic-

ally obscure, no pollen; 3, richly organic,

pollen present (5 cm); 4, richly organic

but very little pollen (7 cm); 5, (4 cm);

6. (7 em) & 7, (5 em), richly organic,

pollen present. Depth of section about

& om.

120 ELIZABETH A, A. GRUBB

valley tloor ——___

cae “OR Kanmantoo schist

stream bed mlm

Fig. 3, Vertical section of east bank of Gorge Creck from valley floor to stream bed, showing extent

of organic deposits. Organic sands are visible for further 26 m downstream. At the left is shown

outcrop of Kanmantoo Schist which probably formed a harrier behind which deposit accumu-

lated.

TABLE 1

Pollen counts from layers 3, 5, 6 and 7 (different

Jorms in descending order of prevalence).

Abundant forms Layer 3 5 6 7

Number of slides counted 10 29 13 10

Casuarina 319 922 278 24

Compositae la} 89 896 30 ft 10

Ib 48 21 6 5

2 (Liguliflorae) 21 4 l 3

Chenopodiaceae 44. 45 44 8

Holoragaceac 58 As 13 6

Gramineae 22 #35 29 9

Ranksla 3718 3 3

Myrtaceae 6 10 5 0

Spores 24 «16 3

Unknowns

Kare forms

Cuallitrichaceae

Caryophyllaceae

Centrolepidaceae

Convolvulaceae

Cruciferae

Cyperaceae

Droseraceae

Geraniaceae

Hydrochuritaceae

Labiatae

Legumirosae—Acacia

—Papilionatae

I+) f+ EI+I LI |

Lilisceae

Potumogetonaccae

Rununculaceae—Clematis

Rutaceae

Thymelacaceace—Pimelea

Typhaceae—Typha-like

Umbelliferae

Diatoms

+) te] | $t++) 44.5) +444

$44) 4444) 4) ot} | 44+

+4+4+ |

“Ta Helipterum, Helichrysum, Olearia type pollen.

Ib Others.

"Very numerous.

slides examined from each layer and, to get

some sort of comparison between the layers,

T have listed in Table 2 percentage representa-

tion of pollen from 10 slides from each Ipyer,

It is clear that the number of pollen present

per slide varies markedly, but the commonest

families are present in all layers. The un-

Knowns, which made up 30-60% of the

counts, appeared to be mostly Cyperaceac and

Juncaceae. Both these families have thin-

willed pollen grains with indistinct markings,

and can easily suffer damage and distortion

duc to partial drying out.

The identification of the pollen to species

level was not possible. Many of the genera

represented are widespread and contain several

species which have very similar pollen and dis-

tributions. Conversely, the pollen from the

deposit was. similar to, but not identical with

locally abundant species. The possibility of

Species evolution as well as movement or

migration needs to be borne in mind.

Casuarina-type pollen is by far the most

abundant tree or shrub pollen in the deposit.

There are three species of the genus currently

found in the southern Mt Lofty Ranges: one

tree (C. wrieta) and two shrubs (C. muel-

lerana and C. striata). The shrub species are

commonest in the wetter areas on infertile

soils, while the tree species is characteristic of

the drier facies of Woodland and open-forest,

With increasing moisture tall eucalypts become

prominent, With decreasing moisture mallee

cucalypts replace C, stricta, A further tree

species, C. cristata, is very widespread in ‘low

woodland’ on the dry side of the mallee forma-

tion in the Murray Plains, I tried to use pollen

size to separate species, but found that this

wus of limited value because the range of size

of the fossil pollen Was considerably wider

than that of the present-day species sampled.

At the present time C. stricta is common on

STRATIGRAPHY, PALYNOLOGY AND ORGANIC BANDS a1

TABLE 2

Pollen present on ten slides front livers 3,5, 6 and

7 frommraiest forms only listed and expressed as

roils und % ).

Toiver 3 4 h 7

No, No, FH Ne No. FD

Casuar(te 315 a2 308 41 244 S50 Qa is

Composite ts a 42.68 244 #3 WwW 6

ih au + *) oo

Zz 4 é 2 * » 3 3

Chenpedivesne 44 4 mod NF 8 5

Halorupucese sf 6 92 4 3 4 i 4

Gramineoue my 2 w 2 9. 7 » 6

Banksia 31 # a | 2 sf 31 2

Myriiceae fh */ a! | tow —_-_—

Spores at 2 nu —_*— 1 3

Li kouwes 343% 45 248 43 4a 30 wa OU

Totulss io 770 444 160

" Spores. were found om thiy duyer bur nat on the slides

counted,

;Prabably Included Casuarina and Morivphyllam geains

foo poorly preyveeved ta ideinify accurately,

Probably luceely Cypeimceae and Juneuceac

the racky slopes around the study site, and

the simplest interpretation of the pollen record

is that a similar type of woodland persisted

throughout the period represented by layers 7

to 3, However, the contribulion of Cusuarina

(9 a pollen assemblage iy usually out of all

proportion to its importance m a mixed stand

of trees, so that its apparent dominance of the

local tree flora 8000 vears. ago should not he

liken ats proven,

lwo Ranksin species ure found in South

Australia, Both are largely restrieted to arcas

with rainfall in excess of 400 mm per year,

A marginara is widespread in the Mt Lofty

Kinves, and is Known pear the stuly site,

whereas &, oynata is of more local occurrence

in this part of the State, and is not knawa

neal the study site, The pollen size of the two

species appears lo be significantly different

(Cookson & Erdtmunn 1952). By erarpinati

averaging 34 pm and B, ornate 58 pm. My

fossil material compared closely with A. rar

whom on average of 38 jm was obtained for

12 prains, Th seems likely (hat the pollen is

laruely from A. nwrginata-ype plants. Unlike

Casuarina, fanksie is a poor pollen-prodiucer,

and the relative hundance of Bankyia pollen

sigwests Chal the genus was locally common,

The farnily Myrtaceae, at important family

because of Ts dominance of much of the Aus-

tralian tree flora, ie represented by a remark-

ably low pollen count; cucalypts ure now hy

{ur the most common trees in the area within

au few kilometres of the site. The Myriuecie

pollen in the deposit seems to he mostly from

eucalypts, and to represent a number of spe-

cies. Eucalypts now logally domnant are

known to have high pollen yields (Boomsma

1972) and, in view of the current close proai-

mity of the trees to the site, one would have

expected 4a more obvious record of their

presence.

Chenopodiaceae, Composilae and Grami-

eae are all now found in ‘woodland to open

forest wilh an herbaceous understorey’ (Specht

1972). The importance of the Muctuations in

number of each group is obscure. Pollen from

low shrubs such as Acacir und Piinelea are

also present,

‘Unknowns! play a prominent part on the

pollen counts. The majority of these pollen

were probably Cyperacead and Juneaceae with

possibly some Gramineae, which would be

consistent with a valley-bottom sedge and rush

communily, Typha-type pollen were noted in

very large numbers in layer 6 and, if this iden-

tification is correct, it seems likely that this

species colonized the site for a relatively brief

period, presumably because local conditions

were suituble for ils establishment, Whether

this was a chanee occurrence or dependent on

certain specific ecological factors is Uncertain,

Tr seems likely that the Haloragaceae pollen

recorded consistently from cach layer ts

Myricphyllum. a genus found locally with

several aquatic or marginally aquatic represen-

jatives, This Would be consistent with results

found from other sites of similar age from

southeastern South Australia, Dadsan (18740,

1974b, 1975) noted persistent! high counts for

Mvriophviivie pollen in bis material fron

Lake Leake, Marshes Swamp and Mt Gam-

bier

The precise identiticalion of the different

types of Spores has vet to he realized, but there

are probably at least 10 species fy the depesil.

A number of these are fern spores lacking a

perispore with affinities to Chefhinthes and

findsaea. Two other spore-types were iden-

tified as Anthocerotales, a group: found oeca-

sionally in damp areas higher in the Mr batty

Ranges but not now found i the Palmer area,

Two Lyecopadiim spores were also noted,

although they could not he positively identified

as being from one of the species wow found

in South Australin CL. deaterodenvam, L

laterale and Ly sérpentiniuan) This genus now

has avery restricted distribution Ta the stite,

and is found only ala few sites such as Square

Water Hole, Mt Compass and the MI Lolly

Summit Swamps, all places with permanent

standing water,

122 ELIZABEINM A. A. GRUBB

Discussion

It fas been established by others that the

climate in southerh Ausitalia bas been. rela-

hively stable over the past 10000 years; tem-

perature and rainfall are thought to have been

marginally higher hetween $000 and SOOO

years B.P. than now, and thes spell was

apparently followed by a drier peri around

3000 years B.P, before it became wetter apuin

(Bawler et al, 1976),

'| appears that the generic content of the

vegetation al Gorge Creek has remained

largely unchanyed over the last 3000 years,

Casvarina, Banksiu and Eucalyplus formed the

most prominen: pollen-cantubuting genera

8000-6600 years ago, An understorey of herbs

und subshrubs {chenopeds, compasites and

grasses} was present around yu shallow lake or

waterhole with Cyperacese and Jouneny species

near the water's edee. In the pool grew Myrie-

plydium. Poetamegeton and several other

hydrophyies. On nearhky slopes, possibly

among rocks, were established a few ferns,

Anthoverotales and possibly Lycopadlunt spe-

vies. Only the Anthoceratales jind Lyeapartini

species are no loriger found locally,

The major plant families at this site are also

the commonest families noted hy Dodson

(1974a, 1974b, 1975) and by Dodson & Wil-

son (1975) at five sites in southeastern South

Australia dind southwestern Victoria, All of the

“Noctoriin sites are i areas domimated by

woodland or open-forest and, although the

relative importunce of the major floristic

eroups varies qlite considerably, it is clear

thal the pattern of vegetation at this site is

closely comparable with (hat at sites in the

southeast. It is quite different from that found

by Martin (1973) th material from Nullabor

Caves where the present rainfall is whour 200

mm per year; chenepods dominated her pollen

coumis, while Compositae. Gramineae and

Myttacese accounted for most of the rest of

the pollen.

Pollen analysis shows little change in the

generic conient of the four layers cxamined.

The presence in quantity of the Tvpha-like

pollen in lager 6 would appear to he 9 local

phenomenon, 4 chance oecurrence made pos-

sihly by some change in the local environment,

Fluctuations in climate were apparently noi

efeal cnough fo cause significant changes in the

vevelation, although pollen-contsining sedi.

ments represent only w small part in the his-

tory of the sediments,

ft appears that the onset of wu. slightly dner

climate (perhaps about 5000 years B.P, as dis-

cussed by Churchill 1968, and Bowler er al.

1976), possibly coupled with a step in the

Vegelationul succession af the wateshole

whereby it was no longer permanently wet but

only seasonally swampy, meant that anaerobic

conditions Were no longer maintained, and any

Organic matter formed was no longer pre-

served to form obVious organic bands.

More recently weiter conditions have pre-

vailed again, amd the organic content of the

sediments has increased, as some sort of

ground wover, presumably largely Cyperaceac

and Juncus, has heen established and mnin-

tained, but conditions suitable fer the forma-

tion of permanent standing water or the pre-

servation of pollen have nof re-oceurred, Sands

with a marked dark colouration have accumu.

lared, hut no peat,

One of the most interesting features of the

deposit is the occurrence of spores of the

Anthocerotalés, a group which appears to he

ubsent from the area new, Dodson (1974h)

found an abundance of ‘Anthoceros’ spores in

material from abour 8000 B.P. at Lake Leake,

and there Were nohceable peaks in (he abun-

dance of the genus at Marches Swamp and

Bluc Tea Tree Swamp about 7500 years B.P.

(Dodson & Wilson 1975), and at Lake

Keilambete about 6500 years B.P. (Dodson

1974a), Tt is tempting to suggest that the

mcrease in importance of the Anthocerotales

about 8000-5000 vears B.P. may have been

correlated with slightly wetter conditions.

However, one species of Anthocerotales has

heen recorded in the Wyperfield National

Park in western Vietoria where the rainfall is

about 300 mim per year (G. A. M, Seott, pers.

comm, ), and some species are known to deve-

lop tubers, and appear to be able to withstand

drought (Goebel 1905), Until the spores can

be more positively identified, and more is

known ahour the distributions of the genera

and species and the factors controlling their

growth, one Cannat use them as uneduivocal

evidence of climatic change.

Acknowledgments

lum grateful to my superviser, Dr R, 'T.

Lange, and to Mr PL Lang (Department of

Botany, University of Adelaide) for their

encouragement and critical discussions in the

preparation of this paper, and I gm particu-

larly indebted to my husband, Dr P, I, Gruhb

STRATIGRAPHY,

(Botany School, University of Cambridge) for

his unflagging support and unstinted helpful-

ness, without which this paper would never

PALYNOLOGY AND ORGANIC BANDS 123

haye been completed. The radio carbon dates

were provided by the D.S.I.R. Nuclear Science

Laboratory at Lower Hutt, New Zealand.

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Micro-

GEOLOGICAL HISTORY OF THE MOUNT GAMBIER VOLCANIC

COMPLEX, SOUTHEAST SOUTH AUSTRALIA

BY M. J. SHEARD

Summary

The Mount Gambier Volcanic Complex comprises a close-knit series of composite maars with a

complex history of eruption, the earlier date being 4720 + 90 years B.P. Detailed field mapping has

similarly revealed two main periods of eruption, each one comprising at least three phases of

activity. Maars were the major volcanic structures produced; however, Strombolian and Icelandic

eruptions are indicated by scoria cones and lava sheets.

GEOLOGICAL HISTORY OF THE MOUNT GAMBIER VOLCANIC

COMPLEX, SOUTHEAST SOUTH AUSTRALIA

by M. J. SHEARD*

Summary

SHearp, M, J, (1978) Geological history of the Mount Gambier Volcanic Complex, southeast

South Australia, Trans. R. See. §. Aust. 102(5), 125-139, 31 August 1978.

The Mount Gambier Volcanic Complex comprises a close-knit series of composite maars

with u complex history of eruption. Carbon 14 dating indicates two periods of eruption, the

earlier date being 4710 + 70 years B.P., and the later date 1410 = 90 years B.P, Detailed

ficld mapping has similarly revealed two main periods of eruption, each one comprising at

lenst three phases of activity. Maars were the major Yolcanle structures produced; however,

Strombolian and leelandic eruptions are indicated by scoria cones and lava sheets.

Fach period of activity began with a highly gas charged magma eruption producing vitric

tuffs. Ground water was the major hydrothermal fluid source, the gas being mainly steum.

Closing stages of these periods are marked by low volatile magma eruptions due to the deyhdra-

tion of the proximate country rocks.

There is no evidence for the caldera-collupse on which earlier writers had placed so much

importance,

Recent seismic activity in the aren, including two tremors in May and July 1976, may

indicate that this volcanic province has not yet become entirely inactive.

Introduction

Mount Gambier forms part of a western

extension to the Quaternary Newer Voleanics

of central and western Victoria (Fig. |). This

voleanic centre and that of Mount Schank, 15

km south, are the youngest volcanoes in South

Australia and possibly even southern Australia,

A group of yolcanoes 35 km northwest neal

Millicent (Fig. 1) comprise L6 eruptive centres

and, according to Solomon (1951), Sprigg

(1952), and Firman (1969), are much older,

However, definite ages are unknown and they

may range from 10° to 20 000 years B.P.

The aim of this paper ix lo present recent

observations on the Mt Gambier Volcanic

Complex in relation to current theories on val-

canic structures and styles of eruption,

Previous investigations

Father Tenison Wood's journal, published in

1862, is the earliest surviving work which dis-

cusses the volcanics at Mt Gambier, his conclu-

sions being that the volcanic structures there

were produced by caldera-collapse and multiple

eruptions.

H. Y, L. Brown, Government Geologist, in

1884 delivered a report to parliament dealing

with the geological phenomenon at Mt Gain-

bier, He added very little to Wood's observa-

tions but, supported the collapse theory as a

mode of formation, Further work Was carried

out by Howchin (1901). He concluded that

there had only been one period of eruption,

und agreed that collapse had produced the

large openings in the craters,

Stanley (1909, 1910) desenbed in detail the

petrology of the lava flows, and the ultramafic

xenoliths contained within the yolcunies.

Numerous papers were written on the urea

between 1910 and the early 1950's but these

failed to shed new light on modes of formation.

The first radiocarbon dating was carried out

by Fergusson & Rafter (1957). They dated

charred wood fragments found at the base of

the tuff layers. Two samples taken from two

sites 8 km apart gave different uges, the older

of which was 4710 * 70 years B.P, and the

younger 1410 * 90 years B.P. Blackburn

(1966) considered that us the two samples

Were treated similarly and recent carbon con-

* Flat |2, 15 Statenborough Street, Leabrook, 8, Aust, 5068.

126 M. J, SHEARD

Cur GRAHAM

oe QCAMPBELL HILL

IRHEAD (=)

MAMUIR TRS, sa McINTYRE

t COBOYCE HILL

Millicent " MT BURR(.)

MT FRILLO MT EDWARD

i=]

MT LYON

MT ‘KDOKOUT ey ‘\

OMT WATCH

Tantanoola

AS {Mount Gambier

yaad

Cc, Rar )

ea Point

we sy

Cc. aay es

«J >

1a0°40"

KILOMETRES 5& 20 MKILOMETHES

SOUTH AUSTRAL} .

Basaltic ash, agglomerate

Basalt lava

Fig. 1. SE portion of Lower South East of South Australia showing Quaternary volcanic deposits.

GEOLOGICAL HISTORY OF TEE MT GAMBIER VOLCANIC COMPLEX 127

tamination could be ruled out, the two dates

may record two main periods of eruption,

A major breakthrough in structural jnter-

pretation of voleanocs like those of Ml Gam-

bier came with a paper by Ollier (1967)- He

demonstrated that volcanves similar to Mt

Gambier were not collapse structures but con-

structional features called maars. His proposed

definition of a muar is as follows.

‘Maars are lundforms caused by volcume

explosion and consist of a crater, which

renches or extends below ground level and

is considerably wider than it is deep, und

a surrounding mm constructed of muterial

ejected from the erater,’

In sudition he farther enlarged on this defini-

tion by explaining that calderas generally have

diameters in excess of 5 km and are composed

mainly of acid to intermediate yoleanics where

collapse plays a major role. Maars are

smaller and dominantly constructional features

Where collapse pluys a minor role. In maars

the yoleanics are generally basic hur a few

exceptions in South America are of jnter-

mediate composition.

Irving & Green (1976) classified the basall

Javas at Mt Gambier as pepheline-hawantes

Werived by partial melting from nepheline-

hasanié parent material.

A detailed description of the Mt Gambier

volcanics and their eruptive history is set out in

Sheard", All sample numbers mentioned tn this

text refer ta the collection in the School of

Applied Geology, South Australian Institute of

Technology. Adelaide.

General peology

The Mi Gambier area forms part af the

Gambier Embayment of the Otway Basm, des

enbed by Wopfner & Douglas (1971)- A rela-

tively flat resion exhibiling « sémi-Karstic sur

face, no surface drainage pattern, and broken

hy « series of low regulor parallel aeolian sand

dunes, surrounds the edifice of Mt Gambier.

A sequence of sediments was depasited m the

Gambicr Embayment {rom Jurassic through te

Recent times. Table | summarises ages, litholo-

gies. and approximate thicknesses of the Caino-

goie succession near Mt Gambier, Waneerrip

Group and Knight Formation are, according

to Harris (1971). cquivalent names respec

tively far Knight Group aod Tactwanp Porma-

Hen, as ised by Ludbrook (1969, 1971).

Recent yoleani¢ wetivity is recorded locally

by Mt Gambier und the smaller cone of Mr

Schank to the south (Fig. |)

Eruptive history and volcanic stratigraphy

The volcanic stratigraphy and structural dis-

position of the craters and rocks indicate that

two main periods of volcanism took place.

These two periods are characterised by three

major phases of wetivily, cach period beginning

wilh gas charged magna ertiption, dind ending

in gus poor magma eruption,

Second period eruptions were on a much

larger scale and considerably more violent than

those of the first period,

Fragments from the Bridgewater Formation,

Gambier Limestone, and Wangerrip Group

oceur within the volcanics in quantities of 5 to

25%. These fragments were torn from the sides

of the voleahic conduits during the eruption

und ejected along with the volcanic material

Many of these fragments have been contact

allered by the magma’s heat making some of

them harder or softer than their corresponding

parent material,

A description of the three phases, in tum,

within the two Mail periods of eruption

follows.

First Period (4800 vears BPO

First Phase

Prior to eruption the area consisted of a

seTies of morth-west trending purallel acolian

sand dunes S-15 m high, a resule of the

Pleistocene marine regressions (Fig. 2al, The

dune complex is collectively referred to as the

Bridgewater Formation,

First phase eruptions took the form of small

seule maurt production, The intial magma had

to pass through water saturated sediments and

is thought to have become gas charged.

Voluminous quantities of steam released

caused maur construction rather than quiescent

Fissure eruption. These maars had vents 25—

100 m across gnd ramparts 5-10 m_ high,

Direct outcrop evidence for ash spread during

(he first phase ly pot available; however, sec-

tions in the Blue Lake crater provided dyta

allowing extrapolations 1a be drawn for a mini-

mim ash extent (Figs 2b, 3a).

Rjectumenta from this phase form a thin bul

distinct stratum at the type locality of the

Nurses Landing (grid ref, 7467 B, 1175 N),

where it overlies the Gambier Limestone und

*Sheurd, M, J, (1976) The Geological History of the Mount Gambier Volcanic Complex, South-Eust

South Australia, BApp,Sc Thesis, School! of Applied Geulogy, $4. Insiilule of Technolagy, Adelaide

funpublished),

128 M. J. SHEARD

' Prior to

eruption

Periad 1

Phase 2

GRATER

BLUE LAKE CRATER

Perjod 2

Phase 3

(beginning)

Fe) CRATER RIM

[co] LAKES

[i] Peetstocene DUNES.

FE] GAMBIER LIMESTONE,

[MAAR VENTS,

)PRESENT pay,

VENT, FIGBURE,

BASALT LAVA.

fi] ASH & AGCLOMERATE.

=| AGGLOMERATE

Period

Phase

Period 2

Phase 2

(middle & end)

(O] cone rim.

Ee] BASALTIC PUMICE

(SGORIA).

DYKES.

LAVA-FOUNTAIN

ACTIVITY.

(s} Stow Hoves.

Period 1

=4,800y, BP.

Period 2

= 1,410 BP

ERUPTION.

VITRIG—LAPILLI

ERUPTION

Fig. 2. a-h: the yolcanic ejecta and eruptive centres for each phase of the two volcanic periods so. far

evident in relation to present day structure of Mt Gambier.

GEOLOGICAL HISTORY OF ‘THE MT GAMBIER VOLCANIC COMPLEX 124

TABLE |

Stratigraphic sequence in Mie vicinity ef the Mount

Gambier Volcanic Complex (niodified alter Ludhroak 1969,

Harris 1977).

Thick-

Age Unit Teas Lithology

Quuternucy Undifferen- 0-16 m Laminated ash, tus.

tiated ueglomerutes, and luva

volcanics flows.

Quaterbury Bridgewater 0-15 m Lurgely acolianive with

(Piciaias Formation some shelly beds, Often

cere) is well defined fossil

dine systems marking

ald shore lines (Sprigg

1952),

Oligocene- Gambier 120m Calcilutite-calearenite.

Miocene — Limestane bryozcal and tlinry.

Well jointed and

exhibita Karstic solution

features,

Late Gligo- Compton OS) Fervuginous, rubbly

cene(?) — Coriglo- conglomerate—rework ud

merate Wanucrrip Group kedi-

tricrity.

probably Variable, glauconitic,.

absent silty limestone with

Polished brown igun-

stone grains grading to

brown glauconitic sills.

jvobably Poorly sorted ferru-

Middleto Laeepede

Late Formation

Bocene

Middle to §=Kongerong

Lite Sand absent @inous quarta arenite

Eoorne

Middle Knight M445 m Unconsolidated poorly

Eocene Formation sorted course sand, arit

and interbedded con-

lomerates and car-

bemaceous clays (Marris

1971),

in excess Laminated micaceniis

ef tisim silt. quite sands onc

lwnitic clays (Harris,

1971).

Valeocene Wangerrip

Group

underlies a later lava ow (Fig. 4+). Thicknesses

for this stratum range from 3,5 m at the Nurses

Landing, 2.0 m al the western end of the Blue

Lake, and 0.1 m at the eastern end of the Ble

Lake, Three zones make up this stratum: the

basal zone comprises a poorly bedded country

rock-ash-conglomerate. Rock fragments range

from sill sized to 3 em across; 60% of this zone

consists Of pulyerised Gambier Limestone, The

middle zone contains more volcanic material

than the basal zone anid displays coarse bed-

ding, Finely Jaminated ash ad lapilli-ash Porn

the upper zone. Boundaries between the three

zones are gradational. The basal zone repre-

sents the initial break through to the surface

of the voleanic material, hence the conspicuous

quantity of country reck detritus,

Second Phase

Second phase activity consisted of passive

Icelandic Type eruption of basaltic lava from

both fissures ond pre-existing. vents, Field

occurrences and apparent flow directions tend

to suggest two liva sheets rather than the one

large sheet as proposed by Fenner (1921), ‘The

dunes of the Bridgewater Formation prevented

equidirectional spread of the lavas, confining

them lo the interdunal trough (Figs 2c, 3h),

A second Java flow overlies the eastern lava

sheet—indicating two pulses of activity there

(Figs 2d, 3c}. Heat from the lava baked the

upper surface of the underlying ash layers over

which it flowed. The result is a brick ted zone

of increased competency caused by the partial

remelting of the ash particles (Pig. +),

The basalt itself is grey-blue, fine yramed

with medium grained olivine pheioerysts. It is

generally massive although vesicular and amyg-

daloidal patches. do occur. Original lava flaw

surfaces exhibit rubbly ‘aa’ textures especially

in close proximity to lava caves, Lava ¢aves

range from centimetres to metres across. atid

many metres deep. They crop out at the base

of flows and form by the draining of liquid

lava from a solidified jacket (Fig. 5), Within

the caves drip structures, lava stalactites,

wrinkles and drape structures, give clues to

flow direction and likely source sites (Ollier &

Brown 1965, Sheard*), Figure 6 shows a lava

stalactite (3542) collected from a lava cave;

its base was bent by the moving lava while the

stulactile was still plustic. Thas flow movement

was in the direction indicated by the point of

the stalactite,

One strikingly different lava form, occurring

as float only, is a tachylitic (glassy) basalt (Pig.

7), tTepresenting rapid chilling--possibly by

water in the conduit at the commencement of

lava outpouring.

Major clement wnalvses

sumples ure giver in Tuble 2.

Third Phase

Activity became more violent during the

third phase with the construction of a small

scorn cone at the western end of the area (Figs

2d, 3c, 13—-section B-B’), This eruption was

of the Strombolian type. It indicates that the

geothermal gradient was lowered fallawing the

second phase basalt eruption, thus allowing

some meteoric water back into the system prior

to Ihe cessation of activity,

The scoria (basalt pumice) when fresh

exhibits indescent glassy bubble linings, How-

ever. eam passing through the scoria curing

eruption has oxidised most of the material to

a terra-cotta red colour, destroying the bubble

linines, Gutcrop of this ejectamenta forms a

of four basalt

130

SCALE km

SCALE km,

M. I, SHEARD

VERTICAL EXAGGERATION Y

tV/H = 5-5

METRES

100

PHASE 3

(LATE)

PHASE 3

f |earty)

PERIOD 2

=1,410 y.B.P,

PHASE 2

-- 1

PHASE 5

PERIOD 1

=4,000 y.B.P,

PHASE 1

ASH & AGGLOMERATE. FEEDER PIPES.

Pa] BASALT Lava. WE LAVA FOUNTAINS,

BASALTIC PUMICE v< GEOLOGICAL BOUNDARY,

(SCORIA),

AGGLOMERATE. J CRATER OUTLINE

VITRIG-LAPILLI-TUFF, © — LAKE LEVEL

Sections a-g are atructural projections onto the tine XY

on the plan opposite, (not to same scale).

) PRESENT DAY.

Fig. 3. Cross-sections indicating active conduits and spatial arrangement of the volcanic ejecta for each

phase of the two eruptive periods so far evident in relation to the present day structure of Mt

Gambier.

GEOLOGICAL HISTORY OF THE MT GAMBIER VOLCANIC COMPLEX M34

TABLE 2

Major-element chemical analsex by XRE (uncurrecied)

of four basalt samples taken front the ve lava flaws

of period 1, phase 2, Samples housed ii Applied

Geology collection, School of Applied Geology,

NMAGT., Adelaiile.

ROCK TYPE—Alkuli Oliving Busalts.

LOCALITY—Mount Gambier, S. Aust.

SAMPLES 35141 as15 4514 3540

Si0..% 45.5 44-8 45.3 44.4

Tia % 25 25 25 24

AlyOy% 136 14.0 14.9 15.2

Fe 04% 124 12 12.2 124

MnQ% 11h 0.18 0.17 o.ts

Mg0% #5 83 TR 78

Cal) 104 y.1) 9.0 10.2

Na 9 4.0 49 4.0 5.1

K.0% 24 26 31 7

PLO. %% 0.67 0,91 0.96 0.60

CtiOy% om a.02 a1 o.01

L.OL. = 0.63 2. 0.16

GOL, 0.34 _ 0.07 _

TOTAL — 10.05 10.04 99.94 100,10

L.O.) —Loss on ignition, equivalent to volute loss,

G.O,L——Gain on ianiion, equivalent ta mineral oxida

Hon, Anulysis by ACLS. Laboratories Pry Lod, Unley,

S.A,

Propuralione-crushed wre pulverised pack

SAMPLE LOCALITIES (from Fig. 12)

Sahiple Tasting Northing

3510 7953 LOO

3313 TRIS 1200

3514 1967 hi75

3540 7892 iin

steep chil produced by later valeanie abrasion,

Within the scoria exposures are caverns—one

OL which is known locally as Bootlace Cave,

Second Period (1500 years BoP.)

Second period volcanism was much more

violent and was charged than the first period,

producing much more volcanic detritus. Ollier

(1967) has classified this type of eruption as

pheeatic and il can be likened to the efferves-

cence produced when soda water is uncorked.

During the 3300 years between the first and

second periods, ground water in the country

rocks percolated down earlier volcanic con-

duits. Apparently this meteoric waler was cons

verted fo superheated seam when it reached

the hot magni, possibly located in dykes as

propesed by Con (1975), Remelting may

have been induced by this influx of water inte

u high lemiperature system af partially solidified

basic magma; certainly jt Would have tade the

magma less Viscous and wWiereased its drive to

escape the confining rocks,

(as drilling is the most likely mechanism by

which the magma made its way to the surface,

This process can he likened to sand blasting,

producing # cylindrical conduit which becomes

funnel shaped close to the surface.

New active vents were evolved which blasted

their way through the basalt caps of the first

period, Lurge blocks of basalt and limestone

were thrown out, some weighing in excess of

20 tonnes. Such large blocks and smaller

bombs create piercement structures. tn the ash

layers when they land (Fig. 8). A second feu

ture of the second period cruptions is ¢ross-

bedded ash and dune structures within the ash

(Fig. 9), Aceording to Moore (1967) and

Ollicr (1974), crossbedding and dune like

structures can be produced by base surge,

phenomenon associated with a vertically

directed explosion column, and sweeping across

the underlying surface at high velocity, racial

to the explosive column. Evidence of rainwater

affecting the tuffs is shown in Figure 10 where

two fossil stream channels were exposed by

road widening of the Crouch Street cutting

ferid ref, 8085S E, 1205 N), Rain is pften

associated with voleanic eruption due to the

large quantities of water vapour yeleased from

the vents,

First Phase

The first phase eruptions of the second period

began at the sites of the present-day Blue Lake.

and al two sites along the Razorback (ridge

between the Valley and Leg of Multon Lakes}

(Figs 2c, 3d, 13—sections C-C’ & D-D'). 'Vuaff

ugglomerates were the major type of volcanics

erupted; these are Very poorly bedded near (he

craters but become finely laminated ash and

lapilli-tufls away from the rims, These volcanics

are indistinguishable from later sinyilar eyecta

their extstence has been inferred from struc-

tural evidence.

Second Phase

Volcanism of the second phase was on a

lirger scale than any previous eruptions and

represerits the stage where uctivity reached a

maximum, Composite or grouped maars were

produced at the present sites of the Blue and

Valley Lakes (Flex 2t, 3e). These were formed

by the coulesctng of mtany smull conduits as

they were gbraded wider. Although great

voliumes Of gas Were released by these vents, the

Magy seedis to have been lower in volatiles as

more daplli and ash were ejected, A lowering

vf the volatile content in the Magni sugeests

cithee that the hwiling off of volatiles in the

GEOLOGICAL HISTORY OF THE MT GAMBIER VOLCANIC COMPLEX

magma Was reducing the gase content ur that

the proximate country rocks were drying out

because of the geothermal gridient set up near

the. conduits. Some combination of these

mechanisms is also probable. The second pro

cess would have prevented additional steam

from entering the system,

‘Tuff-agglomerates are by far the most

voluminous of the vuleanic detritus. Struc-

turally there are (ManyY distinee — tuff-

agylomerates; however, texturally and conrpasi-

tionally they are all similar. Where two of these

overlap or intertongue jt is inipossible to dif-

ferentiale between them Hence the descrip-

tions will be yveneralised to cover these vol-

ecanics tis a whole

Bedding es so ponr within the craters that

dip and strike megsurements are impossible to

obtain, thus acctirate eruptive sites cannot be

plotted, The tulf-agglomeraltes are unsorted;

particle sizes runge from silk to holders in

excess oF 2m across,

The components of the tufl-ugglomerite are:

fl) country rock fragments—CGuambicr Line-

stone, diagenetic flint and mareasite

{33

und deep basement rocks—colleetively

15% to 20%

(27 Volcanic detritus—volcanic bombs (olivine

and basalt) — - Ste ta 10%

—lapilli, cinders, and ash 970% to 8Q%

Regression analyses applied to hore hole and

exposure thicknesses indicate that the voleynics

thin exponentially away from the craters.

Lhird Phase

Cessation of uctivity from the Hlye and

Valley Lake maars must have allowed the geo-

theymal gradient to decrease, m turn allowing

{he meteoric water back into the surrounding

rocks, Eruption from the site of the present day

Leg of Mutton Lake crater occurred wtter this

influx, waler being so abundant that the ush

and large ejecta were deposited in a damp

condition, The cooling effect of this water on

the ascending magma may account for the

small size of this crater That is, the magma

Wiis induced to set in the conduit wfter only a

shovt erliptive eycle (Piys 2g, 38). To the west

conlinued actevity from the Brownes Luke

eraler resulted in the creation of two different

ash types. A double maar system is ploposed

nodules (both from the Gambier Line

stone), dolomitised Gambier Limestone,

Wangerrip Group rocks (contact ullered),

ws the generator of these pyroclastics which

intermix along their south-westean boundary

(Figs 2, 3f, 12, 14). The westernmost of the

Outcrop just wbove the Nurses Landing showing baked upper surface of first period—first phase

ash layers in contact with eastern basalt Lava sheet. To tbe felt the basalt displays an autos

brecciated base, a result oF movement after partinl solidificntion. Length of hammer (centre) ty

- One of large lava caves in eastern lava sheet, just south of the Nurses Landing, approximately

10 m deep and 2.5 m wide, A natural Jandshde during July 1977 has totally destroyed this

A fine cxample ol a tava stalaetite (3452), lying on its side, collected from a large cave (arid

ref, 7849 B, 812) N), Jt was attached to the poof, the point of attachment being at the left of

fizure. As the lava drained out of its lava tube, Moid lava still clinging to the rouf dripped uff

onte the flaw tn this case the upper portion had set while the base remaining, plastic For longer

the flow by the flow, Thus it shows one way of determining

Photomicrograph (under plane polarised light) of a thin-section cut from ihe only sample

(3516) of tactrylitic basalt from the aren displays one large bleb of glass, The glass exhibits

perlitic cracking and, where it forms the matrix, it has devitrified ta o magnetite bearing mese-

, One of the many sedimentary structures exposed in the Grouch Street curing: this piereement

or impact structure represedts u block of tuff which Was ejected Irom the erulers and fell onto

. Crossbedded ash and lapilli tuffs in the Crouch Street cutting; this fleure represents an area 4 m

x 2M, Base surge turbulence is the most likely Mechanism by which structures like this are

produced, Overlying the truncated beds is an antidane, one of many exposed at this loculity-

‘Two small fossil stream channels. exposed during road widening in Crouch St. lute 197$/early

1976. Such channels were most likely created during « storm that took place while eruption was

in progress, This structure has now been obscured by a retuining wall. The geological hammer

Fig. 4

32.¢m.

Pig. 5

; feature since it was photographed in February 1974,

Fig. 6.

has been bent in the direction 6 The

flow dircetion for lava flows. The ruler below the stalactite is 22 em Jong.

Fig. 7.

stasis. Field af view = 4.0 x 2.6 mm.

Fig. 8

the ash surface, indenting the layering, Length of geological hammer 32 em,

Fig Y

The base surge passed from deft to right in this section,

hin 1D,

is 32 em Jong.

Fig. 1]

Macroscopic bedding in the vitric-lapilli-tutis below Centenary Tower, photograph ca 1940, Ty

Che left cavernous weathering js evident jn several horizons near the top ef the riilge, Directly

ee the Pb id the volcanics reach a thickness of [60 m. The hol in the foreground is the

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AMBIER VOLCANIC COMPLEX

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two maars produced tuff-agglomerate, while

the eastern maar ejected vitric lapilli-tuff. These

latter tuffs were directed mainly to the south

resulting in a high ridge which now forms the

southern rim of the Brownes Lake crater. Cen-

tenary Tower was built at the apex of this rim.

Erosion of the vitric-lapilli-tuffs appears

slower than the remainder of the volcanics due

to their more competent character, although

cavernous weathering is a common feature of

some horizons (Fig. 11).

A further feature of this eruption was the

removal of most of the western crater rim of

the Valley Lake composite maar. Only a few

small remnants of this rim remain (Fig. 12

‘lapilli-tuff’). Instead of a new wall being built

up to bisect the now very large crater, most of

this material back-filled the Valley, Lake crater.

Originally this crater must have been as deep

as the Blue Lake crater to have accommodated

the large quantity of pyroclastic material which

seems to be missing. However, the Valley Lake

does have a floor sloping away from the

Brownes Lake crater, such that the western

shore is shallow while near the eastern shore

it is 30 m below water level (Fig. 13—section

A-A’).

During the eruptions at the Brownes Lake

crater, two dykes were emplaced within the ash

layers of the southern Valley Lake crater rim,

near what is now called the Devil’s Punch

Bowl (grid ref. 7905 E, 1130 N) (Fig. 2g).

These dykes carry the only lherzolite (olivine

+ orthopyroxene and clinopyroxene) xenoliths

known in basalt rock from this area. All other

lherzolite occurs as bombs or float, thinly

coated with lava or as free chunks within the

volcanics, Over 25% by volume of material

comprising the dykes consists of lherzolite

blocks 5—SO cm in diameter. The dykes are

approximately 20 m long and 50-120 cm wide.

Jet-black basaltic pumice forms the bulk of

these dykes. Dense material such as lherzolite

would naturally settle out in a magma chamber

—hence its late stage appearance, enclosed in

basalt, may indicate a depleting magma reser-

voir, Road works in 1969 temporarily exposed

the dykes but they are now obscured by a

sealed road.

A short phase of lava fountain activity with-

in the Brownes Lake crater brought major

activity to a close, Activity of this type is really

a continuation of the eruption from the

Brownes Lake maars (Figs 2h, 3g). It indicates

virtually complete degassing of the magma,

allowing eruption of lava rather than lapilli or

ash. Lava fountains built up small spatter piles

of ropy lava and small ropy lava flows. Lava

associated with this sort of event is very fluid

and chills rapidly—preserving forms like

twisted rope and fresh cow dung. Numerous

spatter piles have resulted in a very irregular

floor to the Brownes Lake crater. This floor is

atypical of maars which generally have fiat

floors due to gas fluidisation (quicksand effect),

as described by Ollier (1974).

Late stage fumarolic activity is indicated by

the presence of blow holes, the largest of these

being still observable in the Devil’s Punch

Bowl. Three others occur between the Brownes

and Valley Lakes, while three more occur out-

side the main volcanic vents. The latter three

occur within the city of Mt Gambier and repre-

sent the only activity outside the main volcanic

vents (Figs 2h, 12). They form a linear trend

which may indicate their close association with

a near-surface dyke. Conical in shape, these

depressions represent steam discharge accom-

panied by a small quantity of ash and country

rock ejection. The largest blow hole in the city

was used as a rubbish dump prior to 1939; now

completely filled it serves as part of the City

Council Depot in Crouch Street.

Present day

Ash extents are shown by Fig. 15. This map-

ping was carried out using natural exposures,

hand augering and sewerage trench logs, and

the boundary is based on the points where vol-

canic ash merge with the Pleistocene dune sands

or recent soils—thus making visual separation

of the two impossible. With the aid of micro-

scopic and geochemical analysis Hutton et al.

(1959) have shown that the distribution of fine

volcanic ash in soils around Mt Gambier is

much more extensive than is shown by Fig. 15,

The author found fossilised Banksia leaves

within the ash layers near where they pinch out

against the Pleistocene dune sands. These

leaves are indistinguishable from modern day

local Banksia leaves.

Weathering of the volcanics has produced

very fertile soils which are dark brown in

colour and loamy in texture. Soil profiles range

from a few centimetres in thickness at the

crater rims to 0.5 m on the plains.

The complete geological record is displayed

in Figs 12-14. The crater wall profiles (Fig.

14) were compiled from strip photography and

geological mapping; topographic control for

Figures 13 and 14 was taken from Map 1 in

Sheard*.

137

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REFERENCE

Fa Area covered by

J observable tuff.

+ Crater rim

ypreeent

day.

__ Area covered b

geology map (Fig 12),

*— Railway.

—~< Road.

Map showing extent of volcanic material that can be differentiated from soil and Pleistocene

sands with the naked eye. Mapping was carrled out using natural exposures, road cuttings, hand

auger holes, bere logs and sewerage trench logs.

Fig. 13 portrays subsurface volcanic conduit

breccias which do not crop out anywhere at

Met Ganthier. One Mines Department bore log

from a hole drilled in the Leg of Mutton Lake

crater indicates the conduit contains poorly

sorted material, called tuffisite—similar to that

described by Ollier (1974), The other conduits

are ussumed to conta similar material, These

breccias would, according to Ollier (1974),

grade into massive basalt at depth, The

Brownes Lake crater conduit breccia would be

complicated by small feeder pipes to the tate

stage lava fountain eruptive centres,

The future

Recent scismicity in the region of Mt CGiam-

bier suggests that all the activity has not yet

ceased, McCue (1975) has sammurised the

earthquakes that have occurred in the South-

east of South Australia. The first recorded seis-

MTicity was centred at Ningston in’ May [897,

tremors being felt for five hours, causing walter

spouts and sand volcattoes. on the beaches of

Beachport, Kingston, and Robe. In 1948 Rebe

was again shaken by an earthquake of magni-

tude 5.6 on the Richter scale, More recently a

series of tremors has shaken areas closer to Mt

Gambier, In November 1975 a Richter magni-

tude 4,5 tremor occurred off-shore from Car-

penter Rocks only 37 km from Mt Gambier. In

1976 two tremors were recorded: the first in

May had a Richter magnitude of 2,0 and its

epicentre was below the Mt Gambier Volcanic

Complex. The second happened during the late

eVening Of July 12th; it registered 3.6 on the

Richter scale, and local people reported feeling

it. An epicentre for this quake was tentatively

put at | km northeast of Mt Schank and at a

depth between 4 km and 30 km (McCue 1976,

pers. comm.).

Some interesting facts are the time span of

3300 years between the two eruptive cycles so

far evident, and the 1500 years since the Jast

eruption, There is every possibility of a magma

source at depth which may lead to the poten-

nal of geothermal energy exploitation or more

cruptions, At present the Bureau of Mineral

Resources (B.M.R.), Canberra, is conducting

au geothermal study of the Mt Gambier region

GEOLOGICAL HISTORY GF THE MT GAMBIER VOLCANIC COMPLEX

with two aims: firstly to obtain regional heai

flow data from whieh crustal temperature pro-

files cary be extrapolated; secondly to examine

the geothermal energy prospects associated with

the recent volcanism (B.M.R, 1977, pers,

comm, ),

Only close monitaring over a Jong period ol

time will provide factual data, upon which

sonnd conclusions can be divawn as to whether

the recent seismicity heralds further vol-

canicity, or is just regional settling.

Acknowledgments

The author wishes to thank Dr C, D. Branch

for Nis guidance during the carly stages of

research and field mapping, His vast experience

in voleandlogy was an imvalvable aid in direct-

ing the author lo the most productive avenues

of study, Drs A. S. Joyce and R, G. Wiltshire

are thanked for their opinions and advice con-

cerning the petrology of the area, The author

149

is tndebred us the State Lands Department for

survey data, and to Messrs K. McCloy and M,

Zeman of S.A.LT School of Surveying tor the

use of @ steridmetrograph, without whieh a

revsonable topographic map would not have

heen available. For permission to enter the

Blue Lake. the use of a boat and assistant, sind

the loan of E. & W.S. maps, the writer thanks

Mr 1D. Ide, Regional Engineer E. & W.S. Dept.,

Southero, Mt Gambier, Valuable assistance wis

also supplied by the Mt Gambier Branch of the

State Mines and Energy Department, and in

particular the then resident geologist, Mr S.

Barnett, who gave the writer access to unpub-

lished reports, maps, and bore logs, Also

generous assistance was given by Mr F, Aslin

who supplied ash deposit information from

sewerage tench logs if his possession, Finally

for their critique of the original manuscript the

author wishes to thank Drs J. B, Jago and C. D..

Branch aid Mr J, D, Waterhouse.

References

Buacksuen, G. (1966) Radiocarbon dates relating

te soil development and volcanic ash deposi-

tion in South-Eust South Australia, Ans J,

Ser 29, 50-52

Brown, H. ¥. L, (1884) Report on the Lakes in

the Mt Gambier Region, 8, dust, Parle Pap.

256, 2,

Fennex, C. (1921) The craters and lakes of Mt

Gambier, South Australia. Trata, R. Soe. 5.

Awest. 45, 169-208

Fracusson, G. T. & Rarren, T. A. (1957) New

Zealand C1! ave micusurements, N.Z. J Sev

Teehnal. 38001. 732-733,

Firman, J. B. (1969) Quaternary Period. fr.

Parkin, L. W. (Bd.), “Handhook af Sauth

Australian Geology”. Cieul, Surv. S. Ayal,

204-233.

Gunn, P. J. (1975) Mesozeic-Cainozoic tectonics

and igneous uctivily: Southeaslern Australia.

J. peal, Soc, Ausr, 22, 215-22),

Harms, W. K. (1971) Tertiary Siratiasaphic

Palynology, Oiway Basin, fy Wopfner, tL &

Douglas, 1, G, (Rds). Che Utway Basin of

Suutheasiern Australia, Spee, tall nent,

Survs S. Aust, & Wier, 67-7.

Hower, W. (1901) Fxting volcanoes of Mt

CGiumbier and Me Sehank. Yew, Ae New ¥

Aust, 25. 54-62-

Hurrrow, J, T., Blacknunn, G. & Crakke, ART

(1959) Identification of volegnic ash in sails

near ML Gambier, South) Austeptia Mifd 82,

95-98,

Irving, Ad) & Cinves, DLW. (1976) Creocleanis:

try und Petrogenesis of the Newer Basalts of

Victoria and South Australla J weal Sor

Aust. 23, 45-6h.

Luprroox, N, H. (196%) Tertinry Perrad. ta

Parkin, TL. W. (Bd.), “Handbook of South

Anstraling geology’. Geol, Sure. SS. Aust,

177-203.

Lupsroog, N, H, (1971) Stmtigraphy ang Curre-

lation of Murine Sediments in the westem

part of the Gambier Embayment, /n Woptner,

H, & Douglas, I. G. (Eds). The Otway Basin

of Southeastern Australia, Spee Bull. geal,

Sarva §, Aust, & Viet, 47-65,

MeCur, K.P. (1975) Seisoiivity and seismic risk

ja South) Australia, Univ, Adel, Dept Physics,

68 pp,

Mrnore, J. ©, (1967) Base surge in recent volcanic

eruptions. Bell. Poleanal, 30, 337-363.

OLileR, C. D. (1Y67) Maars: Theti characteris

tics, varieties and definition. /bid, 31, 45-73,

Ovier, C. BD. (1974) Phreatic Eruptions and

Maars, dn Civetta, L., Casparini, P., Luongo,

Ct. & Rapolla, A, (Eds). “Physical Vol-

cunology.” (Elsevier, Amsterdam), 289-310,

Onur, C BD. & Brown, M. C, (1965) Lava

Cuves of Victorian, Bull, Valeatiol, 29, 215-

233

Parkin, 1. W. (Rd.) (1969) “Handbook of South

Australian evology.” Geol. Surv, S. Aust,

Sucomon, M. (1951) The volconic deposits of the

South-East of South Australia as sourees of

quarry stone, Min, Rev. 93, 133-137

Spriog, R. C. (7952) The Geoloey of the Suuth-

Fas! Provence with special reference to

Quaternyey coast line migrations and Mader

beach developments. Bull, geol, Surv, 8, Awst.,.

29, 3)-42.

Staneny, FR. ¢1909) Complete analysis of the

Me Gambier basalt with petrographic desorip-

lions. Tras. R. Soe. 8 Aust. 33, 82-100,

Srancey, & RB. (4910) Cherzolite and olivine from

Mt Gatnibier. hid, 34, 63-68.

Woons, J.B. T. Ch862) “Geolagical observations

in South Australia principally in the district

soull-easst of Adelaile’ (Green, |ongman,

Roberts & Civenc. Lomlon & Melbonrne),

404 pp.

Worrsnk, Ho& Daueras. 7. G. 1971) The Otway

Hasit’ af Southeastern Australin. Spee. Bull,

weal, Save S, Aust & Kien, 464 pp,

ARCHAEN TO EARLY PROTEROZOIC BANDED IRON FORMATIONS IN

THE TARCOOLA REGION, SOUTH AUSTRALIA

BY S. DALY, A. W. WEBB & S. G. WHITEHEAD

Summary

A minimum metamorphic age of greater than 2400 Ma is inferred for two banded iron formations

outcropping within the TARCOOLA 1:250 000 map sheet area. The age obtained is considerably

greater than that of the mid Proterozoic Middleback Group with which both iron formations have

previously been correlated. At least two periods of iron formation deposition therefore occurred in

the Gawler Craton during the Precambrian.

ARCHAEAN TO EARLY PROTEROZOIC BANDED IRON FORMATIONS IN THE

TARCOOLA REGION, SOUTH AUSTRALIA

by 8. Dacy*, A, W. Weest, & S. G. WHITEHEAD]

Summary

DaLy, S., Wess, A. W,, & Werrenean, S G, (1978) Archaean to early Proterozoic banded

iron formations in the Tarcoola region, South Australia, Trans. R. Sac, S, Aust, L215),

141-149 31 August, 1976-

A frinimaum metamorphic age of greater than 2400 Ma is inferred for two banded tron

formations outcropping within the TARCOOLA 1:250 000 map sheet area. The age obtained

is considerably greater than that of the mid Proterozoic Middleback Group with which both

iron formations have previously been correlated, At least two periods of iron formation

deposition therefore occurred in the Gawler Craton during the Precambrian.

Introduction

The TARCOOLA 1;250 000 map sheet urea

lies within the northern part of the Gawler

Craton (Thomson 1976), an area of crystal-

line basement stabilised in the Precambrian

(ca 1500 Ma) and now partly covered by sedi-

ments of Permian to Recent age. The oldest

rocks are quarizo-leldspathic gneisses with

interluyered quartzites and thin discontinuous

banded iron formations. Foliated granitic rocks

also occur within the gneiss complex, Basic

and ultrabasic rocks. (Warne 1970!, 1972*;

Holeapek 1972") containing anomalous base

metal concentrations occur within the quartzo-

feldspathic yneisses and may either be con-

formable or cross-cutting; complex structure

and poor outcrop associated with extensive

weathering obscure stratigraphic relationships.

Overlying the quartzo-feldspathic gneisses and

associated hasic rocks 1s a gently folded sedi-

mentary sequence, the Tarcoola Beds, which

has subsequently been intruded by acid vol-

canics and 1480 Ma high level granites

(Blissett 1975, 1977),

Geological mapping of the TARCOOLA

1;:250 000 map sheet area began in July, 1974,

as part of a systematic regional mapping pro-

gramme of the Gawler Craton. Directly related

{0 this Mapping programme are current joint

South Australian Geological Survey and

Amdel geochronology projects, which are pro-

viding radiometric age limits for important

stratigraphic units in the crystalline basement.

In 1975 an age of 2350 Ma was established

for gneissic granites outcropping in the Glen-

loth Goldfield area, 25 km southwest of Kin-

goonya (Webb & Thomson 1977), A similar

age was also determined for a small gneissic

vranite outcrop 17 km West of Tarcoola. These

results prompted further sampling of gneissic

rocks in the TARCOOLA sheet area; at ML

Christie and 6 km north of Kenella Rock

Hole (Fig. 1), Both localities were chosen in

an attempt fo date the associated interlayered

banded iron formations,

The term “iron formation” is used here in

a lithological sense only and does not imply

stratigraphic formality or specific genesis, i,

the iron formation is simply an iron rich rock.

Any formal name to be established in the

future will refer to the enclosing gneisses; the

iron rich horizon or horizons will be included

in this unit.

* Geological Survey of South Australia, Box 151, Eastwood, S. Aust. 5063.

! Australian Mineral Development Laboratories,

17 Warne, S, B. (1970) Mulgathine, Examinntion, Mining Lease 333. Report by Kennecott Explorations

(Aust) Pty Led. $8. Aust. Dept Mines eny, 1375 (Cunpubl,).

2Waine. S. B, (1971) Mulgathing Examination, Mining Lease 491. Report by Kennecott Explorations

(Aust.) Pty Lid, S, Aust. Dept Mines env, 1510 Cunpubl.),

“ Holeapek, F, (1972) Geology of the Hopeful Hill Area, S. Aust. Dept Mines env, 2071 (unpubl.).

8S. DALY, A. W. WEBB & S. G, WHITEHEAD

142

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ARCHAEAN TO EARLY PROTEROZOIC BANDED IRON FORMATIONS IN 5A. 143

The fron formation at Monnt Christie

Loéation

The tron ftorniation oliterops at Lat,

30° 18°33" and Long. 133°30'55" on the west

ern edge of the TARCOOLA 1:)250 000 map

shect area, 28 km north of the Transcon-

tinental Railway (Fig, 1)

General geology

The itou formation outcrop ts a linyered

quartz-henmatite (murlite)-goethite yneiss. tt

lorms a prominent elongate hill surrounded by

surficial scree, sand and mulga seruh, Nearhy

outcrop is poor, often very weathered and

consists of low isoluted bills of quartz-feldspar-

hiotite-garnet-gneiss and schist, and quartz

feldspar-biotite-garnet-cordicrite gneiss with

traces of sillimanite,

The iron formation was. formally defined

as the Mi Christie Metajaspilite by Whitten

(1968). Mowever, regionally the unil may be

one of a number of iron formations.

Srructaral relationships

The iron formation, which outerops over a

distance of O.5 km has a north-nurtheasterly

trend. dips steeply west and contains numerous

small (olds with axes plunging gently northerly.

A Very Weathered coarse-grained massive to

poorly layered quartz-feldspar gneiss siruc-

jurally anderhes the iron formation, The struc-

(ural top, however, is obscured by talus, Rela-

tionships with other iron formation autcraps,

occurring to the north and southeast. are not

known with any certainty because of surficial

eover and camplex simictnre

A detailed aerempgnenc survey (Warne

1970!, 19712) shows that the jron formation

outcropping af ML Christie may he a portion

of the western Himh of a complex untiferm

(Gerdes 19754) with ao north-northeasterly

trend and a northerly plinge (Peg. 1). Linear

magnetic anomalies indicate three and possibly

four magnetic horizons, probably all of which

are handed iran formations. ‘The proposed

structure tm intersected hy the Mulgathing

Trough, a major graben with 4 northwest trend

(Nelson (976).

lithology (CDI, CD22)

Th 19464, two fully erred holes (CDI, 2)

were drilled through the wot formation

(Whitten (965°) perpendicular oo strike, 100

m apart and depressed 40" casterly (Fig. 2)

‘The purpose of the holes was lo investigate

the magnetite content af the tron formation at

depth, Drill core from both holes has provided

Fresh tnaterial for geochronology

The iron formation, approximately SO m

thick, 18 a quarlz-nagnetite-diopside-hyper-

sthene-umphibole gneiss and is generally well

layered with a charucteristig greenish-black

and white banded appearance, The magnetite

layers are slightly discontinuous and of vari-

able thickness, duc to micro-folding, The

layers average 6 mm in width and are inter-

layered with bands of quartz and pyroxene

averaging 12 mm. As the magnetite content

decreases, banding hecomes less distinct. The

iron formation retuins a predominantly grano-

blastic texture even though there is evidence

of a ater phase of metamorphism accom-

panied by reerystallisation and replacement of

some pyroxene by amphibole.

The tron formation contains laminae of

teldspat, cither microcline or plagioclase, and

accessory apatite and iron sulphide. Interbeds

up to 0.5 m thick of poorly Tayered foliated

quartz-feldspar gneiss also occur and contain

varying proportions of biotite and minor gar-

nel, They are occasionally associated with very

thi) magnetite-pyroxene layers and rare, thin,

mussive calcite bands contaming some

pyroxene and pinkish garnet.

A coarse-grained ~~ pinkish-grey, — poorly

layered to massive quartz-plaginclase-micro-

cline -cordierite -garnet gneiss structurally

underlies the banded iron formation. This rock

also contains minor ilmenite and traces of sul-

phide (pyrrhotite, chalcopyrite and a minute

trace of pentlandite), These — feldspathic

gueisses also show evidence of later deforma-

Nin ond retrograde metamorphism. ‘There has

been extensive granulation and recrystullisation

along grain houndaries anc) movement along

small shear planes, Garnet has heen replaced

wholly or qartly by fine grained biotite, and

sillimanite has developed along grain bhorm-

dates in The cordienite-hearing cocks.

Age

Eleven samples of core from CD1 and CD2

were analysed by the Rb-Sr technique (see

Anpendix), OF these, four were quartz-micro-

cline - plagioclase - biotite = eneiss interlryered

“ Gerdes, R.A. (1975) Geophysical appraisal and inierpretation of the detwiledl aeromagnetic duty in

parts of Capiding, Coates, Muckanippie, Mulgathing, Wyobring 1:63 360 sheet areas in the norihwes-

tern cornet of the TARCOOLA 1:24) 000 sheer ar’a. S. Aust. Dept Mines (umpobl) repr 75/14,

TWhitten. G, Te

Dept Mines funpubl} rept #0/42-.

(1965) The investigation of iron formations in the Mulgathing District S, Aust.

144 S. DALY, A. W. WEBB & S. G. WHITEHEAD

MI! Christe (Projected,

D.0.H.co1__

SY NOTE: Trand of

section is 105"

NOTE

D.D.H.CD2 js located 100m

alang strike south af D.D.H CDI

P1728/76 Geachronology sample 7 N SP Hi7 dm 350

»,

LEGEND oto scate) Meters

Very weathered mica schis!

Medium to coarse grained quartz hematite

magnetite pyroxene gneiss, thin schist

interloyers.

Medium to coarse grained, well layered

and distinctively banded quartz pyroxene

and magnetite gneiss.

Quarlz pyroxene magnetite gneiss

containing small interbands of

quartz—teldspar gneiss.

Very coarse grained poorly layered

plagioclase micracline garnet cordierise

biolite gneiss.

METRES

$13138 S.A. Deparlment of Mines and Energy Drn, LP VY

Fig. 2. Cross section through the banded iron formation at Mt Christie.

ARCHATAN TO EARLY PROTEROZOIC BANDED IRON FORMATIONS IN S.A. 145

TABLE |

Rb-Sr datas Mount Christie

SAMPLE NUMBER DEPTH im) LITHOLOGY Rb/Sr Rbs7/Srst *Gr87/Sy5ti

PI7I8/76 CDI 7102-7112 i O70 2.06238 0.7754

PI721/76 CD} F2,.75-72.85 A 0.631 1.8329 U.7687

P1722/76 CD 75.29-75,.36 A 0,806 2.3449 0.7846

P1723/78 CDI 76.05 -76.20 A 0.701 2.0376 U.7753

Pi728/76 CD YF TS-BABS Cc O.U701 ),2025 O7114

P1729/76 CDI 94,49-94 59 Cc 0.573 1.6632 0.7612

PI731/74 CDI 98.49.9667 A 0.500 1.4503 O7535

Pi733/7h CDI 100-64-000.71 Dn 413 1.1949 1.7444

P1735/76 CDI 105.54-105,66 b 0.367 1.0631 0.7405

P1748/76 CD2 £9.71-89.81 A O.906 2.6388 0.7962

P1749/78 D2 91.69-91.80 A 0.663 1.9265 O.7718

with (he quarte-magnetile-pyroxene gneiss and

the Yemaitider quartz-plagioe|aye-microcline-

cordicrite gneiss underlying the tron formation.

The Rb/Sr analyses (Table 1) were re-

gressed and produced # Model 3 isochron of

2417 & 59 Ma with an initial ratio of 0.7036

+ 0.0015, The MSWD of 3,35 indicates that

there is litle Variance beyond that due to

‘experimental error, The isotopic age represents

4 minimum metamorphic age for the rter-

layered iron formation. The low initial ratio

indicates that the material bad not resided in

the crust for more than [00-150 Ma before

metamorphism occurred (Moorbath 1976),

Recently the International Uniow of Geo-

logical Sciences. Subcommission on Precam-

brian Strativraphy (1977) assigned an age of

2500 Ma for the Arehaean-Proterozoic boun-

dary: “The particular tinie chosen is one

which provides a reasonable and practical basis

fur the grouping of geologic events in most

regions of the world and for continent to con-

tinent correlation’. On this basis, the oldest.

recognisable metamorphic uge of the banded

iron formation is therefore assigned to the

eatly Proterozoic, The depositional age of the

iron formation, however, may be Archaean,

The fron formation near Kewella Rock Hole

Loeation

The iron formation outcrops at Lat.

30°S55'23", Long, 134°57'57" on the caster

edge of the TARCOOLA 1:250 000 map sheet

urea, 7 km south of the Earea Dam Goldfield,

und | km nerth of Kenella Rock Hole (Fig,

3).

General gvalogy (Fig. 3)

The iron formation in oulérop is a poorly

lnyered quartz-hematite-goethite rock, Nearby

wulcrop, both to the north and south, is

pinkish-white to grey, well foliated, poorly

banded quariz- microcline= plagioclase gneiss

containing subordinate biolite, chlorite and

garnet. The quartz-feldspar gneiss is intruded

by non-foliated dykes and plugs of gabbro and

dolerite and pinkish massive granite. Dykes of

the Gawler Range Voleanics (Blissett 1975)

runging, from acid to hasic, intrude both the

quartz-leldspar gneiss, ihe basic dykes and,

rarely, the massive granite. The relationship

between the metabasalt (in the N.W. of Fig,

3) and the quartz feldspar gneiss is uncertain.

Structural relationships (Fig. 3)

The iron formation (oc. |) is locally tightly

folded and has a moderate southerly dip, Wis

interbedded with well layered, very Weathered

gneiss, and is structurally underlain by a pink-

ish, well foliated quartz-feldspar gneiss.

Approximately. five hundred metres to the west

(loc. 2) the banded won formation outcrop

is more linear and trénds east-west with a steep

southerly dip. No pink quartz feldspar gneiss

outcrops at this locality.

The exact relationship between the struc-

tural top of the iron formation and the pinkish

feldspar gneiss outcropping further to the

south cannot be established because of paucity

of puterop, Local faulting and basic dyke in-

trusion have further complicated the relation-

ship. Surface mapping, therefore, is unable to

prove whether the iron formation is part of

the Well foliated gneiss sequence, or Whether

it is part of a younger sequence,

Drilling has now resolved the problem, Tn

1973, Abadon Holdings N.L. (Holeapek &

Benbow 19745) in search of base metals,

reenrded the quirty-hematite-gocthite outcrop

of the weathered iron formatiot) as a gossan,

“ Holeapek, F. & Benbow, M. ©, (19745 Geology of the Kenella area. S. Aust. Dept Mines env. 2276

funpubl,}.

146 S. DALY, A. W. WEBB & S. G. WHITEHEAD

Q P1455/76 a 24, : 3

~ Sy

aN area Dam |

icp

Soline and gypsiteraus

clays and silts

Volcanic dykes;

Rhyolile ta basalt, (Evy)

Reddish nor—toliated

granile\Ex

Dolerite and gabbre dykes, co LA |

Amphibole plagioclase pyroxene

meéta—basall. (PABV) —

PAL

ee ee

is)

Quarta micracline plagioclase

gaiget gneiss

Quallz mognehle pyroxene

grens— BILF. AR

inset only,

ARCHAEAN

TO EARLY

PROTEROZOIC

P1456/76

Geochranology sample loculily_ ©

Location at Diamond Drill Hole. —_e

KILOMETRES

0 1 2

5.4. Deparimen! of Mines and Enelgy Di HV. \ DALY, 1977?

Fig. 3. Geological map of the Kenella Area.

ARCHAEAN 1O EARLY PROTEROZOIC BANDED IRON FORMATIONS. IN S.A. 1/47

Several soil peochemical anomalies and ground

magnetic anomalies were recorded in the area.

Nine holes were drilled in the immediate

Vicinity of the outerop and drill holes i, 4 and

9 penetrated unweathered iron formation

(Fiz, 3). Recent logging of this core indicates

that the pinkish quartz-feldspar gneiss is inter-

layered with the iron formation. The iron [for-

mation is therefore part of a quartz-feldspar

gneiss sequence which hos w general east-west

trend and a southerly dip.

Approximately 10 km west of Kenella Rock

Hole is.a small isolated oulerop of iron for-

mation, trending easterly and dipping ver-

lically, which may also be part of the quartz-

feldspar gneiss sequence (Fig. |),

Litholeey (DDH, 4, 9)

The iron formation, which has a maximum

thickness of 25 m, ranges from a very poorly

layered to a well Jayered greenish quartz-mag-

netite-pyroxene (diopside and hypersthene)-

amphibole gneiss. The magnetite bands of the

well layered gaciss ave 2-6 mm wide tind are

interlayered with quurtz-pyroxene bands which

range up to 40 mim in thickuess.

The iron formation contains laminae of

feldspar interyrown with the magnetite and

mafic minerals, and bonds of well luyered

pinkish = quartz-microcline-plagioelase — gneiss

containing varying proportions of biotite: and

subordinate garnet, This gheiss is ussociuted

with thin calcite jayers contyining miner

wwiphibole, pyroxene, olivine and garnet, The

iran formation also contains bands of eenerully

Very poorly layered greenish-grey quartz-

feldspar (predominantly plagioclase) gneiss

containing abundant relic garnet and some

sillimanite, The greyish gneiss in DDI No, 1,

from 143.1 m to 146.2 m, ¢ontyins ) small

umount of sulphide with Cu 150 ppm, Ph 350

ppm, Zn 2.1% (Holcapek & Benbow 1974°%),

Both the pinkish quartz-microcline-plagioclase

meiss and the greenish quariy-plagioclase-

garnel-rich yneiss ulso accur above und below

the banded iron formation, The greenish

quarlz-plagioclase gneiss is very readily

weathered near surface, whilst the pinkish

eneiss is far more resistant, Which Would exe

plain the dominance of pinkish quartz-feldspar

gneiss in outcrop,

The iron formution und assovinted lelsic

layers in part retain a granoblastic non-foliated

texture! however, there is evidence of a Juter

episode of retrograde metamorphism accom.

panied by teetonic stress. This event has

restilted in the partial or complete replacement

of pyroxene hy amphibole, of garnet by

chloriic und biotite, reerystullisation of much

of the quartz and feldspar to u finer grain size

and the development of a foliation,

Age

Fourteen samples of pinkish quartz-feldspar

gneiss, from the more boldly ouleropping area

approximately 6 km north of the iron forma-

tion, were collected for isotopic dating, (Fig.

3), Outerop near the iron formation is poorer

ufid More Weathered, Material from the drill

core Was not used because of extensive [rac-

turing, Nine samples were analysed by the

Rb-Sr technique, Although of acid compusi-

tion, all samples had a low Rb/Sr ratio which

precluded the production of a precise iso-

chron (Table 2), The analyses with the excep-

tion of sample P1458/76 produce a linear

army, Regression of the eiht samples com-

prising the array shows that there js still a sig

TABLE 2

Rb-Sr data: Kenella Area

SAMPLE NUMBER LITHOLOGY Rb/Sr RbS7/Sr8h 3 S87 /Srsh

Pldd7/76 A 0,604 24173 0.7739

P1448/76 A 0.755 2.1941 0.7772

PT450/76 A 0.846 3470K 0.7930

P1451/76 A (3605 3.9949 R459

Pias4/76 A 250 9.7245 0.7284

PI45S/7é A 0.620 {BOIS 0.7675

P1456/76 mn 0,980 28549 T8025

PL458/76 A 1315 3.8386 0.8192

P1459/76 A 0.93) 0.8416 01.7307

A Quartz-microeline-plagioelase-biotite gneiss

B GQuartz-microcline-bidtite cneiss, .

C Quartz-phigioclase-cordierite biotile eimeiss.

D Quartz-microcline-plagioclase-garnet-biotite gneiss,

* Measured ratios normalised to Srkk/Sphh =

B.3752

148

ihificant scatter of the data above that expected

[rom expermentsl error (MSWD 14.3),

The isochrou (Model 4) yields an age of 2488

+ J30 Ma with an initial Set/Sr ratio af

0.7014 ~ 0,0038 using the decay constant

Rb§? — 1.42 % 10°! y-, The isotopic age rep-

resents a minimum metamorphic age for the

pinkish quartz-feldspar gneiss sequence inter-

layered with the banded tron formation, A

minimum metamorphic age of 2488 = 130 Ma

is therefore inferred for the banded iron for-

mation, On the basis of the previous discus-

sion the metamorphic age of the banded iron

formation is assigned to the beginning of carly

Proterozoic

Conclusions

The banded iron formations near Kenella

Rock Hole and at Mount Christie have a simi-

lar composition, ave and metamorphic history

und are possible stratigraphic equivalents.

More significantly, both iron formations have

) minimum metamorphic age greater than

2400 Ma. Previously, all banded iron forma-

tions within the Gawler Craton had been

regarded as stratigraphic equivalents (Whilten

1966, ‘Thomson 1976). However, initial Sr iso-

topic ratios for units of the Hutchinson Group,

which imcludes the iron formations of the

Middleback Ranges, suggest that deposition

could not have occurred prior to ca 2000 Ma

{Webb 19787), considerably younger than the

metamorphic age inferred for the iron forma-

tions near Kenella Rock Hole and at Mt

Christic. Two periods of iron formation depo-

sition therefore occurred in the Gawler Craton

during the Precambrian; the older iron forma-

tions are now part of the gneissic sequence on

which the younger iron formations were depo-

sited,

S. DALY, A.W. WEHH & S. G. WHITEHEAD

lron formations of both ages outcrop within

the TARCOOLA 1;250000 sheei arca. The

Wilgena Hill Jaspilite (Whitten 1968), a Une-

grained finely laminated quartz, hematite rock,

outcropping 14 km east of Tarcoola is con-

sidered to be Proterozoic in age, Although

high grade gneisses (presumed older base-

ment) outcrop only 6 km from Wilgena Hill,

the metamorphic grade of the iron formation

is probably only greenschist facies, It is thus

strikingly different from the coarse graimed,

twice deformed banded tron formations out-

cropping at Mt Christic and near Kenella Rock

Hole.

The RbSe whole rock ages of 2400 Ma

obtained for gneissic rocks from the Tarcoola

region significantly extend the area of known

Arehaean to earliest Proterozoic basement

from southern Eyre Peninsula, first described

by Cooper er al, (1976) and Webb & Thom.

son (1977). In acklition, gneissic rocks out-

cropping poorly to the north and west of the

Tarcoola region have similar north-northeast!

structural and magnetic trends that ate charac-

teristic of the older basement near Mt Christie

and hence a considerable part of the north-

Western Gawler Craton may be Archaean to

carliest Proterozoic in age.

Acknowledgments

The generous assistance of Mr B, P, Thom-

son of the Geological Survey of South Aus-

tralia both in the field and in the preparation

of the manuscript is gratefully acknowledged,

This paper is published with the permission

of the Director-General, Department of Mines

and Energy and the Director of the Australian

Mineral Development Laboratories.

Appendix

Analytical Methads

Rb/Sr ratios of the powdered total rock samples

were determined in duplicate by X-ray Myorescence

spectrography. Sr'7/Srs" patios were measured on

unspiked samples with a 370 em, 80° sector mass

Spectrometer and corrected for mass discrimina-

tion by normalising Sr**/Sr8" to §3752. Measure-

ments on Eimer and Amend SrCoy, over the

course of several years, give 4 value for Srtt/Se¥

of 0.70802 © 0.00006 (standard deviation of pop-

ulation), Constants used in ihe ase calculations

were:

Rb / REIT 2.600

A Rb‘ = 1.42 & 10 yt

Linewr regression of the analytical data was

made following the methad of Melniyre et al.

(7966) using eslimutes of analytical error of 0.6

fecefliciont of variation based on 67 duplicate

analyses of Rb/Se in the concentration range of 20

to 600 prim) far RbT/Sr8* and 0.05 (coefficient

af variation) for Sr87/Sr&, The erpars quoted are

the 95% confidence limits.

* Webb, A, W. (1978) Geochronalogy of the Gawler Craton. Amdel Report for Project 1/1/1322 {in

prep. ).

ARCHAEAN TO EARLY PROTEROZOIC BANDED IRON FORMATIONS IN S.A.

149

References

BuissettT, A. H. (1975) Rock units in the Gawler

Range Volcanics, South Australia. Q. geol.

Notes, geol. Surv. S, Aust. 55, 2-14.

Buissett, A. H. (1977), GAIRDNER map sheet,

Geological Atlas of South Australia,

1:250 000 series, Geol. Surv. S. Aust.

Cooper, J, A., FANNING, C. M., FLroox, M. M.

& Ouiver, R. L. (1976) Archaean and

Proterozoic metamorhpic rocks on southern

Eyre Peninsula, South Australia. J. geol.

Soc. Aust, 23, 287-292.

INTERNATIONAL UNION OF GEOLOGICAL SCIENCES

SUBCOMMISSION ON PRECAMBRIAN STRATI-

GRAPHY (1977) Minutes of the fourth meeting

of the Subcommission—The John de Villiers

Memorial meeting—held at the University of

Cape Town, Cape Town, South Africa, July

11-15, 1977. Geol. Newsletter (in press).

Mcintyre, G. A., Brooks, C., Compston, W. &

Turek, A. (1966) The statistical assessment

of Rb-Sr isochrons. J. geophys. Res. 71,

5459-5468.

MoorpaTH, S. (1976) Age and Isotope con-

straints for the Evolution of the Archaean

Crust. In Windley, B. F. (Ed.), “The Early

History of the Earth’, 351-360. (John Wiley,

London).

NELSON, R, G. (1976) The Mulgathing Trough.

Q. geol. Notes, geol. Surv. S. Aust. 58, 5-8.

THomson, B. P. (1976) Gawler Craton—regional

geology. /n KNIGHT, C. L. (Ed.), “Economic

Geology of Aust. and Papua New Guinea”.

Vol. I, Metals, Monogr. Australas. Inst. Min,

Met. 5, 461-466.

Wess, A. W. & TuHomson, B. P. (1977)

Archaean basement rocks in the Gawler

Craton, South Australia. Search, 8, 34-36,

Wuilten, G. F. (1966) Suggested correlation of

iron ore deposits within South Australia. Q.

geol. Notes, geol. Surv, S, Aust. 18, 7-11.

WuittEeNn, G. F. (1968) Type section of iron

formations, Tarcoola District. Q. geol. Notes,

geol, Surv. S. Aust, 26, 4-7.

A NEW SPECIES OF HYLID FROG FROM THE NORTHERN TERRITORY

BY M. J. TYLER, M. DAVIES & A. A. MARTIN

Summary

A new species of hylid frog Litoria personata is described from the East Alligator Region of the

Northern Territory, Australia. Eternal morphology and features of cranial and postcranial anatomy

indicate a relationship to the Litoria latopalmata and L. nigrofrenata species groups. The species

lives at the perimeter of the rock escarpment, and breeds in temporary rock pools. The tadpole is

noteworthy for the spectacular gold stripes along its body and tail.

A NEW SPECIES OF HYLID FROG FROM THE NORTHERN TERRITORY

by M. J. Tyter*, M. Davies* & A, A, MARTIN]

Summary

lycer, M. J. Davies, M. & Martin, A. A. (1978) A new species of hylid frog from the

Northern Territory. Trans. R. Soc. §, Aust, 102(6), 151-157, 31 August 1978.

A new species of hylid frog Litvria personafa is described from the Last Alligator Region

of the Northern ‘Territory, Australia, External morphology and features of cranial and post-

cranial anatomy indicate a relationship to the Literia latopalmata and L, nigrefrenata specics

groups. The species lives at the perimeter of the frock escarpment, and breeds in temporary

rock pools. The tadpole is noteworthy for the spectacular gold stripes ulong its body and tail.

Introduction

Although frogs of the family Hylidae are

popularly termed tree-frogs, aumerous species

are wholly or predominantly terrestrial, or else

are scansorial in non-arboreal situations such as

upon exposed rock fuces. In Australia members

of the Literia latepalmara, L. nasuta and L.

rugro/rendta species groups are good examples

of terrestrial species, AJL have rather elongate

bodies, unwebbed fingers, variably webbed tocs

and relatively long hindlimbs.

Vhe terrestrial species occur only in eastern

and northern Australia, One (L. latopalmeata

(Gunther) ) extends into arids parts of westero

Queensland and New South Wales, and

recently hus been collected in the extreme

northeast of South Australia (Tyler 1977),

There remains considerable uncertainty

about the number of species in the L, latepal-

mata group as defined by Tyler & Davies

(1978), The three named species differ

only slightly in colouration and in the few mor-

phological features recognised to be significant.

Biological dula are inadequate to permit

clarification of the taxonomic status to be

accorded to some populations, Similarly the

phylogenetic relationship existing between this

und other species groups has yet to be

resolved

As a result-of the collecting activilies of Mr

Greg Miles of the N.T. National Parks and

Wildlife Commission, we were able to examine

in 1977 specimens of an undescribed species

of Litoria from the East Alligator River region

of the N.T. It bears a resemblance to members

of the L. letopalmeata and EL. nigrofrenata

species groups. Subsequently Davies, Miles, and

Tyler obtained a further adult specimen in

November 1977, Miles and Tyler collected

tadpoles and recently metamorphosed young

frogs in April 1978, and Miles and J, Morris

collected more adults and recently metamor-

phosed individuals in May 1978,

Here we describe the new specics and dis-

cuss its phylogenetic relationships.

Material and methods

The specimens reported here are deposited

in institutions abbreviated in the text as

follows:

Northern Territory Museum, Alice Springs

(NTM)

South Australian Museum, Adelaide (SAM)

Methods of measurement follow Tyler

(1968a) and osteological comparisons are

those adopted by Davies (1978). Tadpoles

were fixed in Tyler's (1962) fixative and

staged according to Gosner (1960),

Litoria personata sp. moy,

FIGS 1-6

Holotype: SAM R.16773. A gravid female

collected at Birndu (12°32'S: 132°8'B), south-

cust of Cannon Hill Station, East Alligator

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

+ Department of Zoology, University of Melbourne.

152 M. J. TYLER, M. DAVIES & A. A. MARTIN

D oe y iota Sohal

Fig. 1. A. Plantar surface of foot of Litoria wotjulumensis SAM R.16857; B. Lateral surface of head

of L. personata; C. Plantar surface of foot of L. persenata; D. Palmar surface of hand of

L. personuta; E. Palmar surface of hand 1. tornieri SAM R,16779.

River Region, Northern Territory,

Davies, G. Miles, and M. J,

27.x1,1977,

Definition: A small rock-dwelling species

(female 32.8 mm; males 28.8—28.9 mm S-V

length), characterised by its unwebbed fingers

with distinctly expanded terminal discs, first

by M.

Tyler on

finger longer than second; moderately long

hindlimbs (TL/S-V 0.51-0.60); broad, dark

stripe on the side of the head; tadpole with

striking, dorsolateral gold or yellow stripes on

the body and tail.

Description of holotype: Head longer than

broad (HL/HW 1.15); head length more than

NEW HYLID FROG FROM NORTHERN TERRITORY 153

one third of the snout to vent length

(HL/S-V 0.37). Snout prominent, projecting

in profile and slightly rounded when viewed

from above and in profile (Fig. 1B). Nostrils

more lateral than superior, their distance from

end of snout two-thirds that from eye. Dis-

tance between eye and naris less than inter-

narial span (E-N/IN 0.86). Canthus rostralis

slightly defined and straight, its nature accen-

tuated by dark rostral stripe. Eye relatively

small and inconspicuous, its diameter equiva-

lent to eye to naris distance. Tympanum

completely visible; diameter slightly more than

two-thirds eye diameter (Fig. 1B).

Vomerine teeth on short, oval elevations

between anterior edges of choanae. Tongue

broadly oval.

Fingers long and slender, lacking lateral

fringes (Fig. 1D); in decreasing order of

length 3 > 4 > 2 > 1. No webbing between

fingers. Terminal discs moderately well

developed, extending laterally beyond lateral

edges of penultimate phalanx. Subarticular

and palmar tubercles prominent,

Hind limbs long (TL/S—V 0.59). Toes in

decreasing order of length 4 >5>3>2>1

(Fig. 1C). Webbing reaching half-way up

penultimate phalanx on toe 5 and below sub-

articular tubercle at base of antepenultimate

phalanx of toe 4. Subarticulate tubercles

prominent. Small oval inner and smaller

rounded outer metatarsal tubercles.

Dorsum very finely tubercular; abdomen,

pectoral region and undersurface of thighs

coarsely granular; submandibular area smooth.

Slightly developed tarsal fold, but no supratym-

panic fold.

In preservative pale grey with a conspicuous,

very dark stripe extending from nostril to eye,

and posteriorly to above insertion of forearm

(Fig. 2). A narrow white stripe from lower

margin of eye to posterior extremity of man-

dible. Ventral surface pale cream.

In life background colouration similarly

grey or pale brown. Ova, viewed through a

transparent portion of body wall, small and un-

pigmented.

Dimensions of holotype: S-V 32.8 mm; TL

15.9 mm; HL 10.3 mm; HW 9.1 mm; E-N

2.7 mm; IN 3.2 mm; E 3.5 mm; T 2.3 mm.

Etymology: The specific name is derived from

the Latin, personatus, masked, in reference to

the dark stripe through the eye.

Variation

There are twelve paratypes: SAM R.16774,

an adult male collected as a recently meta-

morphosed juvenile on Cannon Hill Station,

N.T. by G. Miles in August 1977. This speci-

men was reared at the University of Adelaide,

and preserved in alcohol when it reached

adulthood; SAM R.16775, a sub-adult male

collected with the preceding specimen; died in

captivity; SAM R.16776 (cleared and stained),

Fig. 2.

Live Litoria personata. Paratype SAM R.16774.

1S M. J,

Bradshaw Ck, Cannon Hill,

G. Miles, 2411977; NTM A.123-125,

juveniles, G, Miles, 1.1977; SAM R.16829,

16855—56, metamorphosing juveniles, Cannon

Hill, G, Miles and M. J. Tyler, 26.iv.1978;

SAM R.16830-32, adults and juveniles from

Birndu, G. Miles and I. Morris, 20.v.1978.

The adult males measure 28,8 and 28.9 mm

S-V respectively, and the females 30.6 and

32.2 mm. The cleared and stained specimen

had very large pigmented nuptial pads on the

first finger. The other specimen lacks nuptial

pads, bul possesses a submandibular vocal suc,

The head is elongate and the snout prominent

and tapering in both specimens,

Hind timb length is highly variable, and

proportionately Jess than or greater that that

of the holotype (TL/S-V 0.51-0,60 in the

adult and sub-adult paratypes).

Six of the juveniles exhibit the adult pattern

of markings; the seventh is in a state of

transition, exhibiting traces of the conspicuous

pale Stripes that characterise the tadpole ol this

species (described below).

un adult male,

Larval morphology

Five Jarvac collected at Cannon Hill on

Lit,77 are in stages 27-41; their total length

ranges from 23.7 to 44.1 mm and their body

length from 10.3 to 16.7 mm. Six larvae

collected on 26,iv.78 are more advanced,

including specimens at stages 41-45. Their

total length ranges from 41.8 to 55.1 mm and

their body length from 16.6 to 18.6 min. Fig.

3A shows a larva at stage 41, Dimensions of

this individual are: total length, 52.9 mm;

body length, 18.6 mm; maximum body width,

9.0 mm; maximum body depth, 7.5 mm;

maximum tail depth (including fin}, 8.6 mm.

The mouth is subterminal and the anus

opens to the right of the tail fin. The eyes are

lateral, The spiracle is sinistral and ventra-

lateral; it is nat visable in a dorsal view ot

the larva. In its general body form the larva

resembles those of other Australian ground

hyhds From lotic habitats, eg. Lb. levveurt

(Martin 1967). The body is Nyttened and the

tail fin is narrow, while the tail musculature

is powerful. The mouth structure is also

typical of Australian hylid larvae which live

in Howing water; there are two upper and

three lower rows of labial teeth, and the

papillary border is complete, The horny jaws

ure relatively weakly developed (Fig, 3B).

TYLER, M, DAVIES & A, A] MARTIN

- VA

ON eid: 0

B 7 alae “

Se ayn Aa— %

~~ J san DI nai, ve

ee P aan _ awn aL ne Si, Ly

or. My une

io ma en Heyy, ‘ Mes a

gh hy My

ann enelt = %

a te ee

aniline itty po Rue a Senn nN a ?

Y ane =

ont igs TO - (Narn, Ie eo

= “ie — Pw

. yw Pe

We aw Ruin at

vi ‘Wd at, ve ee, eld

* umm

Fig, 3. A. Lett lateral and dorsal views of larva

of Litoria personata at stave 41> B, Mouth

dise of larva. of J. personara at Stage 31.

In life larvae are dark brown on the dorsal

surface and creamy white beneath. The

dorsolateral stripes are gold to yellow, In

preservative the dorsal ground colour is

greyish-brown. There is an irregular dark grey

transverse band belween the eyes, and in front

of this band there is an arrowhead-shaped

duck grey patch, The dorsolateral stripes and

the ventral part of the body and tail are creamy

white, The tadpole’s striking appearance stems

Irom the dorsolateral stripe, and from the

abrupt transition from dark to light pigmenta-

tion along the lateral midline.

Unfortunately the larval morphology of

otber members of the L, latopalmate complex

hus not been described; hence whether or not

this spectacular appearance is diagnostic of the

larva of Lo perserata is unknown,

Comparison with other species

(a) External merphelogy: The elongate body

form, projecting snout, relatively long hind

limbs, unwebbed fingers and poorly webbed

tocs ure a combination of features exhibited

by all terrestrial Liroria, The extreme of these

NEW HYLID FROG FROM

adaptations is demonstrated by members of the

L, nasuta group in which the elongation of

head, body and limbs is most pronounced.

I northern Australia the L. nasuta species

group is represented by L. nasuta, This species

has longer hind limbs than L. personata

(TL/S-V 0,64-0.78 in L. hasuta; 0.51-0.59 in

L. personata). The head of L. nasuta is pro-

portionately much longer (HL/HW 1.21-1.43

in L. masuta; 1.13-1.17 in L, persenata). The

two species also differ in skin texture: very

finely tubercular in L, personata; with nume-

rous, longitudinally «arranged plicae in L.

nasula.

The sympatric species L. torniert of the L.

latopalmata species group lacks the finger discs

of L. personata (Fig. IE) and has a disrupted

lateral head stripe; the stripe is continuous in

L. personata, The new species may also be

slightly smaller than L. tornieri: S-V of the

female £. persenata are 30.6-32.8 mm,

whereas the range in L. tornieri is 31,1-

39.7 mm. The S-V of male L. personata

(28.8-28.9 mm) ts in the middle of the L.

tornieri range (26.1-32.1 mm).

The habitus, finger discs and proportions

indicate a close relationship between L.

personata and L, wotiulumensiy of the L.

nigrofrenata species group. They — differ

principally in size and colour: L. worjulumen-

sis is considerably larger (males 33.8-37.7 mm;

females 45.7-54.1 mm. Tyler 1968b and un-

published data) has fully webbed toes (Fig.

1A) and often is infused with lemon yellow

on the abdomen, flanks and undersurface of

the lower limbs.

(b) Oyxteology; Provisional comparisons

sugvested that the closest relative of L.

personata is L. woyilumensis, whose skull ts

illustrated by Tyler & Davies (1978). Dorsal,

lateral and ventral views of the skull of L.

persenata are shown in Fig. 4.

in both species the skull is longer than broad.

and the slightly elongate snout is rounded

terminally in dorsal aspects. The nasals are

moderately-sized, narrow, bones very widely

separated medially by the sphenethmoid; they

do not articulate with it. The sphenethmoid is

double and moderately to well ossified: it

projects between but not beyond the nasals,

There is minor variation in the form of the

frontoparietals. They are moderately ossified,

lack unterior contact with the nasals and do

nol overlap the crista parotica posteriorly in

NORTHERN TERRITORY iss

ia ~ 1X

Z~_ln—rp

SI UAU tA rn lh

5mm

Fig, 4. Skull of Literia personata. Paratype SAM

R.16776. A. Dorsal view; B. Lateral view:

C. Ventral view.

156 M. J. TYLER, M, DAVIES & A. A. MARTIN

Fig. 5. Prevomers. A. Litoria wotjulumensis; B.

L, personata,

both species. However, there is a slight postero-

medial articulation in L. wotjulumensis, but not

in L. personata. The frontoparietal fontanelle

is large in both species and is continuous

posteriorly in L. personata.

The crista parotica are moderately short and

broad with prominent epiotic eminences, and

the otic rami of the squamosals do not overlap

the crista parotica. In L. personata this ramus

is clearly separated from the crista parotica,

whereas in L. wotjulumensis the relationship

of these bones is more intimate. The short

zygomatic ramus of the squamosals is longer

than the otic ramus in L. personata whilst in

L. wotjulumensis the arms are of approximately

equal length.

The pterygoid is well developed and the

median ramus is in bony contact with the

prootic. The quadratojugal is well developed.

The pars facialis of the maxillary is shallow;

the well-developed posterior process reaches

the level of the maxillary process of the nasal

in L. personata, but in neither species does it

make bony contact. The alary processes of the

premaxillaries are broad at the base, widely

separated medially, and curve posteriorly after

an initial vertical section. The palatine pro-

cesses of the premaxillaries are well developed

and do not abut medially or at their ex-

tremities.

The premovers are reduced medially, widely

separated, and have short horizontal denti-

gerous processes (Fig. 5). The palatines are

short and narrow.

Fig. 6. Type locality of Litoria personata: Escarpment at Birndu, N.T.

NEW HYLID FROG FROM NORTHERN TERRITORY 157

The cultriform process of the parasphenoid

is extremely long and narrow; the alae are also

long and narrow and are at right angles to the

cultriform processes,

In the post-cranial skeleton the sacral

diapophyses are broadly expanded in L.

personata and moderately to broadly expanded

in L, watjulumensis. There is a flange on the

distal head of the third metacarpal, and the

intercalary structures are ossified in both

species.

Habitat

The holotype was collected ut night upon a

flat shelf on an open rock face at the foot of

the Arnhem Land escarpment; the type locality

is shown in Fig. 6. Tadpoles and metamar-

phosing juveniles were taken in or around

evergreen non-eucalypts, with Pandanus and

shrubs rising to approximately 8 m;: overall

visibility is approximately 20 m.

Acknowledgements

This study was supported by an Australian

Research Grants Committee grant to M. J.

Tyler. Visits to the Alligator Rivers Region

were supported by the Supervising Scientist, for

the Alligator Rivers Region.

We are very deeply indebted to Mr Greg

Miles of the Northern Territory Fisheries and

Wildlife Branch for valuable field guidance and

generous hospitality. Figure | was prepared by

Miss. Kathy Bowshall, and Figure 2 by Mr

Bohdan Stankovich-Janusch.

Finally we are indebted to Ansett Airlines

temporary pools upon the escarpment or at its of Australia for providing in-transit air-

foot. The area supported a ‘Mixed Scrub’ com- conditioned accommodation for the live

munity (Story 1969) composed mainly of specimens.

References

Davies, M, (1978) Variation in the cranial Tyrer, M. J. (1962) On the preservation of

osteology of the Australopapuan hylid frog Anuran tadpoles. Aust. J, Sci, 25(5), 222.

Litoria infrafrenata. Rec. S$, Aust. Mus.

17(22), 337-345.

Gosner, K. L. (1960) A simplified table for stag-

ing anuran embryos and larvae with notes on

identification. Herpetologica 16, 183-190.

Martin, A. A. (1967) Australian anuran life

histories: some evolutionary and ecological

aspects. Jn A. H. Weatherley (Ed.) Aus-

tralian Inland Waters and their fauna.

Australian Natl Univ, Press, Canherra.

Srory, R. (1969) Part VII. Vegetation of the

Adelaide Alligator area, In R, Story et al..

“Land of the Adelaide Alligator Area,

Northern Territory”, CSIRO Land Res. Ser.

(25), 114-130.

Tyitr, M. J. (1968a) Papuan hylid frogs of the

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

‘Tyier, M. J. (1968b) A taxonomic study of hylid

frogs of the Hyla lesueuri complex occurring

in north-western Australia, Rec. S. Aust. Mus.

15, 711-727.

Tycer, M. J. (1977) “Frogs of South Australia.”

(Revised Edition) (South Australian Museum:

Adelaide.)

Tyver, M. J. & Davres, M. (1978) Species groups

within the Australopapuan hylid frog genus

Litoria Tschudi, Aust. J. Zool, suppl. (63),

1-47.

EARTHFLOWS IN THE YANKALILLA AREA OF SOUTH AUSTRALIA:

SIGNIFICANCE OF RAINFALL, SOIL PROPERTIES AND MAN’S

ACTIVITIES

BY W. J. VAN DEUR

Summary

Thirty-three earthflows were located on Permian glacigene deposits east and southeast of

Yankalilla, South Australia. Their formation relates to periods of intense, concentrated rainfall

when excess soil moisture resulted in deformation by plastic flow. Dating of these earthflows

revealed that while all have formed after European settlement, there has been a time-lag between

occupance and the majority of mass-movements. The time-lag resulted from alterations in physical

and chemical properties of the soil over time, leading to a gradual decrease in shear strength. Soil

alterations were initiated by clearing of natural vegetation after settlement.

EARTHFLOWS IN THE YANKALILLA AREA OF SOUTH AUSTRALIA;

SIGNIFICANCE OF RAINFALL, SOIL PROPERTIES AND

MAN’S ACTIVITIES

by W. J. Van DeuR*

VAN Deur, W. J. (1978) Earthflows in the Yankalilla area of South Australia: significance

of rainfal, soil properties and Man's activities. Trans. R. Soc. S. Aust, 102(6), 159-167, 31

August, 1978,

Thirty-three earthflows were located on Permian glacigene deposits cast and southeast

of Yankalilla, South Australia. Their formation relates to periods of intense, concentrated

rainfall when excess soil moisture resulted in deformation by plastic flow. Dating of these

eorthflows revealed that while all have formed afier European scttlement, there has been a

lime-lag between occupance and the majority of mass-movements. The time-lag resulted

from alterations in physical and chemical properties of the soil over time, leading to a gradual

decrease in shear strength, Soil alterations were initiated by clearing of natural vegetation after

settlement.

Introduction

The influence of man on the development of

certain Jandforms is both significant and wide-

spread in many parts of the world, Of particu-

lar importance is the acceleration of the pro-

cesses of erosion resulting from removal of

natural vegetation und the subsequent history

of Jand use,

The Fleuricu Peninsula, about 80 km south

of Adelaide, South Australia, an area cleared

initially in the mid-nineteenth century by

European settlers for the cultivation of wheat,

clearly shows the repercussion of such enter-

prise in the form of gullies and mass-move-

ments. It is estimated that these processes have

together resulted in a reduction of at least

20% in the amount of available, arable Jand

(Campana, Wilson & Whittle 1954). Thus

these processes are of economic as well as

geomorphological interest.

In an attempt to elucidate various aspects of

the development of these mass-moyements, and

in particular the relationship between man’s

activities and landform development, an

investigation of 33 examples of mass-movement

was carried out in an area of approximately

100 sq. km south and southeast of Yankalilla

(Fig. 1).

tier mary s

Yankalilla

earltitiow

rivers

Fig. 1. Location of earthflows.

Found either in isolation or in coalesced

groups (Figs 2 & 3), these mass-movements

are earthflows as defined by Sharpe (1938)

and Vames (1958), whose classifications ate

based on the nature and rate of movement and

the resultant morphological features. The

volume and extent of earthflows varies, but

in all instances movement is restricted to depths

of 5 m or less. Observed variations in profile

are thought to relate to stage of development,

with the mature shape comprising a spoon-

shaped hollow bounded by a steep, arcuate

” Geography Discipline, School of Social Sciences, Flinders University of South Australia, Bedford Park,

S. Aust. 5042.

160

headscarp which becomes more fully inclined

at the foot before bulging above the turf sur-

face ly form an elongate lobe, extendine duwn-

slope (Fig. 2), Developing earthfiows are

distinguished by arcuate tensian cracks tesult-

ing fram subsidence and low level, sub-turf

bulging, Older earthflows Were located,

although in these the main characteristics such

as headsearps and lobes have been subdued by

subsequent Weathering and erosiir.

The majority of carthilows are found on

averdeepencd, glacial depressiovis, filled with

Unconsolidated glacial, flurvio-placial and

placio-tacustring drift of Permian age, resting

unconformably on Precambrian and Cambrian

rock (YANKALILLA and JERVOIS map

sheets. Genlagical Atlas One Mile Series: Gvol,

Surv. S. Aust., Adelaide).

These readily eroded deposits were prutectes|

during the Mesozoic planation by virtue of the

fact thal they lay below the base level of

stream incision (Campana, et al, 195-4),

Evidence for a Mesozoic age for peneplanatinn

is to be found in the presence of a Laterite

cupping of the present plateau surface. ‘This

Jaterite generally has been considered to be of

a Tertiary age (Fenner 1930), but more recent

investigations have pssigned formation to the

Triassic (Daty, Twidale & Milnes L974:

Twidale 197A),

Rejuvenation cesultiag from. Pertiry Fault-

ing allowed rivers such as the Yasikulilles,

Bungala and bunay to cul back inte the upland

regions. Consequently, the Permian glacigenc

deposits were eroded aod transported mure

rapidly than the resistant bedrock, thereby

forming an area of comparatively low cleva-

tion anu relief. Slopes developed on these

deposits are graded, displaying well develnped

pper convexities and [ower concavities, offen

separated by long rectilinear sections with an

average inclination of IN".

The resistant uplanes comprise heavily

metamoarphosed and folded Preeaintrian and

Cumbriun deposits, In detail these consist of a

centvally placed core of Archean micaschists

and gnerses wpon which the deposits of the

Adelaide system rest unconformably. To the

east and south, the Kanmantoo group of prey-

wackes, phyllites, quartzitic schists and

micageous quartzites are found,

Several major problems need ja he con-

sidered in an attempt to explain the develup-

ment of these carthfows. First, the date of

occurrence of each movement must be deter-

mined us tccurately as possible to estabfish

W. J. VAN DEUR

whether they are rehel or modern. Second, in

conjunction with this, it is necessary to show

iF these carthflows are active or dormant, and

hence whether they relate to the present

system of slope processes, or tire evidence of

past slope disequilibylum, Fimally, — their

relabonship net only to the anthropogenic

factor buy also to the geological, pedological

and climatic controls operating in this region

imust be established,

Dating of earthtlows

Since the jnthropogenic factor has been

postulated as.one of the major factors influenc-

ing the development of these earthtiows, it is

«wf some importance to establish as accurately

as possible the date of occurrence of each

movement. Four dating Llechniques were

employed;

1. Acrial photographs (he first of which

were taken in 1949) show the location and

morphology of some of the present earthflows.

However, because mins were not made in

consecutive years, it was possible to ussign a

particular earthflaw to a range of years only,

2. Geological maps of the area (Campana,

etal, 1954) indicate 16 ‘landslides’ but do not

distinguish type, size or piature of movement,

Omissions have been found to oceur when

comparison was jade Wilh the 1949 aerial

photographs.

3. Local residents were interviewed and, con-

sidering the limitations imposed by migration

to and from the area as well as the accuracy

ol memory, much useful information was

obtained, However, for earthflows developed

more than ten years ago, it was only possible

to assign movereots fo a range of years.

4, A. statistical approach based on rainfall

records was used. A recent earthilow was dated

wilh, uccuracy using the methods otitlined, and

from this it wis passible ty calculate the

amounl of rainfull above the median necessary

to produce movement. Years of above median

rainfall were extrapolated to indicate periods

Where earthflowage could have occurred. How-

ever, total rainfall is of less importance than

(he distribution, for when well spaced, excess

wiler can be femoved withoul precipituting

mass-movements (Sharpe 1938; Sharpe &

Dasch (942; Crovier 1969; So 1971; Nilsen,

Taylor & Dean 1976), The rainfall records

Were therefore exarmned for evidence of

unusually heavy concentrations.

EARTHFLOWS IN YANKALILLA AREA 161

Fig. 2. Single earthflow (No. 9) (a) scarp (b) foot (c) lobe (d) toe,

Fig, 3. Coalesced earthflow (No. 20).

Fig. 4. Earthflow (No. 8) Nole the incipient tension crack (a) and subturf bulge (b) to the left of

the main movement, corresponding to the scarp and foot of the main earthflow.

162

TABLE |

Age and Activity of Earthflows

Ref. Age in yrs. Activity Slope

No (from 1978) Angle

l SU-+- b 14°

2 30+ D i3°

3 50+- b 12"

+ 23 A 12°

5 4 A tt!

6 25-50) E 1°

7 ? Db i

8 th) A 12°

9 31 A Lo°

0 ? E 1"

lI 22-23 D 12”

12 4- § A g°

13 7 A 11°

14 $1=32 D 10°

15 r4 A 10°

16 7 A 10°

17 31-32 dD 10°

18 50-+-+ E [5°]

19 50+ D 15"

™) 23-23 A 16°

21 7 A y°

22 7 A 9°

33 25-50 A ge

24 25-50) A 1"

25 ? A 2°

26 10 A 12”

27 25-50 nD 20"

28 20-25 A 1"

29 30-50 dD 10°

30 7 A 7°

31 25-50 E I1°

32 25-50) E 14°

33 25-50 D 5°

mean = 10.8°

S= 92"

A = Active: D > Dormant: E = Extinct.

Twidale (1976) questions such an approach

hecause of the possible variations in rainfall

hetween the recording station and the site of

the earthflow. Three points, however, lend

validity to the application of the technique in

this. instance, First, there are a number of

recording stations within a small area, with

some data extending back over one hundred

years, and use has been made of the records of

local inhabitants to supplement official records

(Mason 19541; Robertson 1975),

Second for the earthllow used as a base, the

rainfall data of a farmer about 0,5 km east of

the carthflow was compared with the official

1 Mason, B.

Meteorology. (Unpublished).

W. 1, VAN DEUR

records and found to be virtually identical. This

is not to suggest that variation is not possible,

but rather that because of the limited area

being considered, this variation is minor, This

dating technique is not intended to be used

alone, but oflers a means of delimiting years

of possible movement Which, when combined

with the other methods, lends a greater degree

of accuracy to the results,

The ages and present state of activity of

earthflows are presented in Table 1, It ix

evident that the majority of movements have

occurred over the last 50 years, with a large

proportion of these post-dating 1945, ‘These

earthflows are generally active or in such a

state-of dormaney that they may be readily

reactivated. For ¢xample when a portion of the

foe of an apparently dormant earthflaw was

removed during road repair undermining and

a consequent surge of the entire Jobe occurred.

The time lag between settlement in 1839 and

the initiation of widespread mass-movement

after 1945 needs explanation. Earthflows

probably developed prior to European settle

ment but on a much smaller scale, as is

evidenced by the fact that no mass-movements

ure to be found on the few remaining areas of

natural Vegetation once common to. the region

(Light 1839). The vegetation consisted of

savanna woodland on the glacial lowlands

(f£ucalyptus leucoxylon; E. camaldulensis and

E, aderata) grading to sclerophyll on the

plateau surface (Boomsma 1948*; Williams

1974). Vegetation was cleared initially for the

cultivation of Wheat but was later replaced by

wattle trees, After 1910 grazing became the

predominant form of agricultural activity

(Pridham 1955"),

Investigation and analysis of earthflow

In order to appreciate the morphology of

earthflows in terms of processes operating, an

investigation of the physical and chemical

properties of earthflow number four was under-

taken, This movement, which was shawn to

have occurred initially in 1955 and developed

to its present slate in 1956, was selected because

it is the largest, single earthflow within the

area (although larger are known to have

(1954) “Clinvatolegical Survey of the Fleurieu Peninsula”. Commonwealth Bureau af

= Boomsma, (1948) Ecology of the Fleurieu Penmsula M.Sc. Thesis, University of Adelnide, ( Unpub

lished).

*Pridham. G. J. (1955) Landuse in the Yankalilla Avea B.A, Hons ‘Vhesis, University of Adelaide.

(Unpublished).

EARTHEFLOWS IN YANKALILLA ARPA 163

humic sand

sond

sandy clay

2 clay with decreasing

z sand content withdepth

< pure clay

ae)

angular debris in

4 clay motrix

Fig. §. Composite soil profile diagram,

existed), and it was known to be stable in the

lobe zone, although minor beadward extension

by means of block slumping does occur.

Stability was confirmed by cyewilness uccounts

(D. K, Crawford, per comm,) and by measure-

ments taken over a period of months in winter,

To establish rates of movement, an highly

active earthflow was selected (No. 8, Pigs 1 &

4). This earthtlow formed initially in 1968, and

has continued to move downslope, as we found

in 1975 and confirmed on subsequent visits in

1976 and 1977. Although smuller overall than

carthflow four, measuring 9) m from scarp

to toe, and 50 m in width, this earthtlow

exhibits the classical morphology of such move-

ments.

A composite soil profile (Pig. 5) was

established for carthflow four by sinking 4

series of auger holes on and adjacent to the

main body of the movement, In all bores the

quart sand layer extends to an average of 1m

beneath which the percentawe of clay iucreases

loa depth of approximately 3,5 m, Below this

a layer of highly compressed ‘pure’ clay is

found, which in jurn is underlain by a zone of

ungilar debris set iv a elay matrix,

Samples were taken al depths of 15 and

Jyh and tested for variations in sund/clay ratio,

and the chemical nature of the clays present

analysed bry means of X-ray diffraction, These

resiilis ave presested in Table 2,

TABLE 2

V-ray oiffraction analysiy

fore |, | 4ii Bore 2,3m_ Bore 3, im

Kaolinite 30-40% 230% [20%

Uite 20-30% 40-40% A000

Quartz {Q-20% 0% [0-20

Montmorillonite

und or randomly

shetrified material 20-30% 20-30% 2W-T0%

Lhe most inportant feature of these results

is the decrease in stable kuolinite and quartz

with depth, while illite and montmorillonite

show un increase. Both of these latter clays are

capable of expansion in [he presence of

moisture, Clay has a low permeability which

would cause ground water to be confined,

allowing time for absorption into the crystal

lattice (this is evident in winter when water

logging of the soils is seen to occur), The

saluration conditions produced by heavy rain-

jull causes swelling and uplift of the over-btur-

den, The jastability of the slope is therefore

increased,

Observations in gullies and man-made cut-

linus reveal the presence of such a clay, of

varying thickness and at differcat depths,

throughout the area. The role of this clay in

the formation of earthllows iw therefore con-

sidered to be of extreme importatce.

The sample from 1.5 m was tested by the

Casagrande technique to establish the Alterberg

limits of plasticity and liquidity. Adopted from

civil engineering, the application of these

techniques to the study of mass-muvements has

been criticized on the grounds that the samples

ure not in situ, However, the amount of

understanding of processes operating derived

(rom the use of the Atterberg limits, warrants

their application (see Crozier 1969), The

liquid limit of the sample was found to be

380%. the plastic limit 13.5%. und the

plusticuy index 245%. These figures are in

accordance with the parameters. sugyested by

Nusmith (1964) for a sandy clay soil formed

cn ghicial deposits (LLL, 41%, PL. 19%),

The water content by weight was found to

be 19.79% af 1.5 m and 32.69% al 3 im. In

both. instances the plastic limit has heen sur-

passed even When Nasmith’s higher figure for

plasticity is applied), and thus deformation by

plastic flow under the influence of gravity miy

be expected. It is believed, however. that this

does not occur tntil higher water contents, such

us occasioned by heavy rainfalls, are

164 W. J. VAN DEUR

experienced, for the slopes upon which earth-

flows are found are of low to moderate

declivity, ranging from 7-16° (Table 1).

Nature and rate of movement

Using the results of the detailed investiga-

tions described above, as well as observations

on other mass-movements in the area a model

to describe the processes operating in the

formation of an earthflow can be constructed.

Heavy rainfall results in the subsurface

eluviation of fine materials which, along with

flowage (probably in the vicinity of the clay

layer) causes a disruption in drainage, leading

to the formation of a ‘soak’, Typically at such

locations the ground surface assumes a hum-

mocky appearance. Such disruption is known

to have occurred at the present location of

earthflow number four as a result of heavy and

concentrated rains in both 1946 and 1947.

Further rainfall accentuates subsurface flowage,

eventually producing a minor subturf bulge.

This flow however, subjects the upper slope

to tension which, when coupled with subsidence

due to eluviation, results in the formation of a

tension crack. Such a situation is currently

evident adjacent to earthflow number eight

(Fig. 4) where the incipient scarp, in the form

of a tension crack, corresponds to the main

scarp, while subturf bulging is in line with the

foot of the main movement. Eventually the

lobe breaks the surface at this location, forms

a minor recumbent fold, and then slides down-

slope on a planar glide surface composed of

vegetable matter and lubricated by water. This

results in the introduction of an auto-catalytic

process, since water tends to accumulate in the

scarp foot depression. This moisture, along with

that which falls directly onto the lobe, is seen

to exude from beneath the lobe at the toe.

The rate of motion of the lobe was

established by measurements taken during

August at three locations along the toe. The

results are presented in Table 3. Taking a mean

of the motion of the three test lines, the rate

of movement is 23 cm/week, or 3.3. cm/day.

However, movement is highly variable in re-

sponse to the amount of rainfall, in summer

the lobe being almost stationary. Observations

in 1976 and 1977 indicate movement is still

occurring and since the slope is constant to

the valley floor, movement will continue until

this point is attained.

The moisture content of samples taken at the

scarp and the toe were found to be 18.5% and

28.13% respectively. The amount of moisture

above the plastic limit (Nasmith’s figure of

19%) is therefore minor, yet movement as

indicated was comparatively rapid, supporting

the hypothesis (Skempton 1964) that once an

earthflow is set in motion, lower water con-

tents than those necessary to initiate movement

can cause a continuation of that movement.

Further, as mentioned, flow is replaced to a

large extent by planar sliding on a _ water

lubricated surface.

Transversely, differential movement of the

lobe is occurring, while a given section of the

lobe moves at varying rates over them. This

variation over time is explicable by reference

to the level of rainfall, but the differential

transverse movement poses a_ problem. It

is possible that variations in the physical

nature of the material occurs, but observations

suggest a homogeneous character. If it is

considered that the energy for plastic flow

is derived from gravity, and that the degree

of energy depends on mass, then where mass

is greatest the energy level is greatest. For

a given area of sliding surface this is where

the lobe has maximum height. The increased

friction expected due to greater mass, is com-

pensated by the lubrication provided by the

water. Mass however is comprised of not only

the materials of the lobe; absorbed water also

increases mass and the higher sections of the

TABLE 3

Rates of Movement, Earthflow Eight

Initial Length Present Length Movement

Line Line Line

1 2 3 1 2 3 1 2 3

S.viii.75 3.05 3.05 3,05 3.05 3.05 3.05 0 0 0

12.viii.75 2.78 2.96 2,53 0.27 0.09 0.52

17.viii.75 2.65 2.71 2.14 0.12 0.24 0.40

22.viii.75 2.53 2.56 1.98 0.12 0.15 0.15

eee

* Observations taken 30.x.75 showed line three to be completely covered. Movement of over 3,05 m has

therefore occurred,

EARTHFLOWS IN YANKALILLA AREA 105

lobe have the potential to retain more moisture.

Once 1 motion these sections of the lobe also

possess a greater energy and thus will continue

lo move afler the cessation of ramfall

Burthflows inerease thew dimensions ufter

the initial flow largely by movement of the

lobe, but feadward extension also occurs. This

is mainly by means of block slumping at the

sean dne to laleral pressure release, hel mary

ulsa over by meuns of secondary eariflow, is

found an earthflow number four in 1974,

Factors producing eqrttillows

In allempling lo assign a process tye miass-

movement, the cuuse of individual carthflaws

is considered, although Varnes (1958) sites:

‘In most cases a number of cases exist

simultaneously und so attemping toa decide

which one finally produced failure is nat only

dilivalt, but also incorrect. Often the fiual fac-

for is no more that a trigger that sets in motion

un carthmass that was ulready on the verge

of failure.’

Wheo analysing earthilows within the area,

a association is established wath high rainfall,

but in fact it is & combination of climate,

ueology, sull properties and the role of man.

All these variables must be considered,

Vor motion to have peeurred. shear stress

must have exceeded shear strenurh, thut is the

resistance af the soil to stress, Shearing strength

ina moemally unconsolidated soil is dependent

Upon the cohesion between soil patticles and

friction due to wrenulor tterlocking of these

particles, A sandy soil which possesses

newigible cohesion, has high levels of internal

friction which in turn allows a high angle of

repose, In comparison clay has low internal

friction but high levels ef cohesion, For slope

fuilume lo oceur, two factors must ac,

singularly or in conjunetions either stress is

increased beyond shear strength, or the latter is

reduced, [no the studly area dhe major cases of

ass-mioverent isa decrease in shear strength,

Short term stresses, such as produced by seis

min ueuviry, were lound to be af Ht ar ne

consequence, However, Joly term. stresses

resullrog from the lowing of soil uring heavy

raintall may be considered a triggering factor

uid therefore relure oto the climutic

vharuteristics of the Mleuricu Peninsula, These

have heen determined from records kept since

about PSA0 both officially anu by local tarners

(Mason 1954; Rohertsun 1975),

Distribution of cainfull fluetuates weearding

to the seuson and with topokruphy, the main

source being frontal uplift during the winter

months which, when acceniuated by topo-

graphy on the western margins of the

Peninsula, results tm annual talls at up te

SOO mm, Wathin the area where the majority

of earthflows are found, rainfall ranges from

5350 mm along the coast in the vicinity of

Normanville to 750 mm near Taman Valley,

Since unusually heavy concentranons of rain-

fall in short periods of time are more likely to

lead fo muss-rhovements, if is necessaly to

know the median aimounts of rainfall, and

relate these to the actual amount which fell at

the time an carthfow was toitiated. Tn winter

the median is 250 mm, while in summer this

Ueecrduses fo 63 mm. (Mason 1954), This sum-

ier figure is of grewler importunce when taken

in conjunchion wilh the amount otf moisture

required to prevent the Juss af soil water

(150 mm), This exeeeds the amourt of rainfall

in the upper quartile tange (125 mm.) so that

summer desicestion is to be expected, ‘The

opening of the surface layers Of sotl is cun-

sidered to be uf utmost importanee, for i

allows the deep penetration of nioisture when

the first rains Full) usually in Apeil,

The major cause of carthtlows is a decrease

in the Shear strength of the soil, anu the shear

strength of these glacigene deposits varies with

sand/chay ratio and the desree of compaction.

The superficial sand layers lack intergranular

eahesion, but are held by interuranular (riehon

uml adhesion by walter Bulking of the sand

allows u higher than normal angle of repose

Which, when coupled with the nun-plastic

nulire ol sam, resulis tn there being no curth-

flows involving sund alone The inereasing elfy

content with depth is fesponsible for the plies

Lic grilles of the soil, and it is a direet result

of u deerease ty cohesion of this clay that

carthflows aceur, A tuidiber of factors are res

pansible for this reduction iu shear strength

die loon gleerease ph cobesion. although the

unthropogenic factor is of utiiost inipartunee.

‘The process ol wetting und drying, which

causes expansion und contraction ef the illite

vod montmorillonite fallice, over lime sig-

nificantly reduces the cohesive toree berween

cluy particles. Desicewtton is 4 common

occurrence during summer months, when

evaporation exceeds precipitation, tet only an

the body of the carthllow, but on the stable

surroutiting: slopes of (he area, Where an over-

hunfowof sand is present. capillary renieavil ol

eromd water is sidlicient to produce sybsurliee

dusivention, Purther, the cohesive strength of

166

clay decrease With an increase of soil moisture,

and thus the subsequent replucement of

groundwater, causes an increase in pore-water

pressures Which brings about a further loss of

cohesion as the normal interpranular forces are

taken up by the witerstitial water, The super-

incumbent mass of soil is therefore partially

supported by this groundwater, resulting in a

further decrease in shear strength,

Failure, us fas heen demonstrated by

Skempton (1948), i8 nol immediate and is

considered to vary with slope, ranging from 6

weeks if the case of a highly colloidal clay

at 90" to 50 years on a clay slope ot

18", Acknowledging the differences in clay type

and proportions, i ts felt that the low slope

angles in the urea contribute lo the time lag

between the clearing of vegetation and earth-

flow.

Cohesion is also reduced as a consequence

ul clearing, as a change to the clay-humus

colloid results from base exchange, Humus has

the impertant role af improving soil texture

and structure by the creation of granular

ugeregates. These aggregates are destroyed with

the loss of humus and the replacement by

sodium ions. More importantly however,

humus has the propensity to absorb 80-909)

of its own weight in water, whereas clays can

absorb only 15-20%. If a sufficient quantity

of humus exists, rainfall is retained in the sur-

tuve layer fo a certain degree, thereby

decreasing the amount of water in contact with

the substratum, Since earthflow occurs at this

level hy plastic deformation, it is probable that

the humus layer slows or prevents the

attainment of plasticity. During summer

inonths, water ts retained by the humus and

thus desiccation i reduced.

It has been suggested that vegetation

‘tabilises slopes hy root anchorage. Various

W. fF, VAN DEUR

studies have indicated the relationship between

mass-tnovements and the depth and type of

root systems (Rice, Corbett & Bailey 1969),

So (1971) however, doubts whether this

relationship is a clear cut as suggested, anil

infers that vegetalion holds only the surface

layers, and allows plastic deformation at a

lower depth.

Within the area under discussion, the role

of vegetation is vitally important. No large

scale mass-movements are discernible on the

little remaining vegetation, although minor

movement has occurred in earthflow number

tWelve, Where isolated trees and gorse are

found. Rafting of trees was limited. Overall,

therefore, earthflows are located on cleared

slopes, while some have heen stabilised by

revegetation,

The time lag between clearing, and sub-

sequent carthflow is attributed to a number of

factors, Because of low general slope angle

Bravilational shear stress is limited. More

importantly, the cohesion supplied by the clay

and clay-humus colloid decreased gradually

ever time by wetting and drying and base

change on the clay-humus colloid. The holding

power of roots was lost at an early stage, bul

earthflow did not occur until shear stress

exceeded shear strength, Increased shear stress

resulted from saturation of the soil produced

by intense rainfall over short periods of time,

Once moVement causes minor subsidence, a

water trap is formed and thus an autocata-

lytic process eventuates, Why an carthflow

occurred al one point and not another may be

related to minor differences in soil profile, rates

of loss of cohesion in clay, the deterioration

of the clay-humus colloid and ultimately the

time of cleuring of vegetation by European

seltlers,

References

Cymiana, B, Witson, Bo & Wairrie, A, WG

(1954) The gealogy of the Jeryois and Yanka

filin Militry Sheets, Rep, Jivest, geol. Surv.

NS. Aitar, 3. 1-26.

Choditn, M, J. (1969) Earthflowe occurrence dim

ing. high intensity roinfull, Engag Geal, 3(4),

4ZS-935,

DaiLy, B, TWipALe, C. R. & Mites, A. BR. (1974)

The jige oF the lateritized summit surface an

Kangaroo tsland ond adjacent areas of 5,

Australia, J. geal. Sve. Aust, 21) 387-392.

physiogriphic features of South Australis.

trans, Ay Soc. Aish, 54, 1-36,

Lisa, W. (1839) “A brief journal of the pro-

ceedings of William Light, lale Sarveyor-

General of the Province of South Australia.

with a few reniarks an some of the objections

that have been made to them." (MacDougall:

Adelaide),

Nasmery, H, (1984) Landslides and Pleistocene

deposits in the Meikle River valley of

northern Alberts, Can: Geeotecl. J, 1(3),

155-166,

Nitsnm, T, H., Tayecn, PL A, & Dran, R, M,

(1976) Natural conditions chat control land-

Sliding in the San Francisco Bay region: an

analysis bused on datn from the 1968-69 and

SAS Ri rainy seasons, US, Geol, Surv. Bull,

EARTHFLOWS IN YANKALILLA AREA 167

Rice, R. M., Corpettr, E. S. & Batty, R. G.

(1969) Soil slippage related to vegetation,

topography and soil in S. California. Wat.

Resour. Res. 5, 647-659.

Ropertson, B. D. (1975) Climatic survey;

Fleuricu. Region 4, S. Aust, Aust. Bur.

Meteorology.

SHarPE, C. F. S. (1938) “Landslides and Related

Phenomena.” (Columbia Univ. Press;

Pageant Books N.J. 1960).

SHARPE, C. F. S. & Doscu, E. F. (1942) Relation

of soil creep to earthflow in the Appalachian

Plateau. J. Geomorph. 6, 312-324.

SKEMPTON, A. W. (1948) “The rate of softening

of stiff fissured clays.” Proc. 2nd International

Conf. Soil Mech. Found. Engr. (Rotterdam)

V.2, 50-53,

SKEMPTON, A, W. (1953) Soil mechanics in

relation to geology. Proc. Yorks. geol. Soc.,

29, 33-62.

SKEMPTON, A. W. (1964) “Long-term stability of

clay-slopes”. (Fourth Rankin Lecture). Geo-

technique 14, 77-102.

So, C. L. (1971) Mass-movements associated with

the rainstorm of June 1966 in Hong Kong.

Trans, Inst. Br. Geogr. 53, 55-66.

TwipaLe, C. R. (1976) The origin of recently

initiated exogenic landforms, 8. Aust. Envir.

Geol, 1, 213-240.

VaRNES, D. J. (1958) Landslide types and pro-

cesses. In E. B. Eckel (ed.) “Landslides and

Engineering Practice.” Highw. Res. Board,

Wash., Spec. Rep. 29; N.A.S.N.R.C. Publ.

544,

WiuiaMs, M. (1974) “The Making of the South

Australian Landscape.” (Academic Press:

London).

STRANDED SHINGLE BEACH RIDGES, UPPER SPENCER GULF, SOUTH

AUSTRALIA: EVIDENCE FOR HIGH WAVE ENERGY DISSIPATION

DURING THE LATE PLEISTOCENE

BY J. R. HAILS AND V. A. GOSTIN

Summary

Stranded shingle beach deposits have been traced over a distance of some 50 km from the near head

of Spencer Gulf southwards along its western shore to Stony Point, near Whyalla. These deposits,

which consist of moderately sorted rounded to sub-angular pebbles and cobbles, form well

preserved ridges 3-5 m above present mean sea level. Entire, non-abraded shells of the estuarine

bivalve Anadara trapezia (Deshayes 1840) are abundant in the beach deposits and, because this

species is now extinct in South Australia, a Pleistocene age is indicated for the ridges.

STRANDED SHINGLE BEACH RIDGES, UPPER SPENCER GULF, SOUTH

AUSTRALIA: EVIDENCE FOR HIGH WAVE ENERGY DISSIPATION

DURING THE LATE PLEISTOCENE

by J, R. HAits* and VY. A, GosTint

Summary

Hains, J, Ry & Gosrin, Vo A (1978) Stranded shingle beach ridges, upper Spencer Gull,

South Australia: evidence fur high wave energy dissipation during the late Pleistocene,

Trans. R. Sac. is. Aust. 102(6), 169-173, 31 Arigust, 1978,

Stranded shingle beach deposits have been traced over a distance of some 50 kni from

near the head of Spencer Gulf southwards along ils western shore to Stony Point, near

Whyalla, These deposits, which consist of moderately sorted, roinded to sub-angular pebbles

and cobbles, form Well preserved ridges 3-5 m above present mean sea level. Entire, non-

abraded shells of the estuarine bivalve Anadara trapezia (Deshayes 1840) are abondant in the

beach deposits and, because this species is now extinet in South Australia, a Pleistocene

age is indicated for the ridgcs.

The movement of gravel by present-day waves in the northern part of Spencer Gulf is

restricted compared with that indicated by the stranded, shingle beach ridges, During the

Pleistocene it appears that the combination of a high sea level, large fetch, strong easterly

winds and high wave energy dissipation along the shoreline emplaced the relict shingle beach

deposits.

Introduetion

Evidence for high stands of sea level during

both the Pleistocene and Holocene epochs has

been cited from several regions of Australia

(Hails 1965; Thom ef el, 1969; Gill & Amin

1975; Thom & Chappell 1975; Cook et al,

1977), Some of this evidence pertains to shore

platforms which may have been abraded

several times during vustatic changes of sea

level in the past, The rate at which shore plat-

forms are modified by marine abrasion varies

widely because of differential weathering and

crosion controlled by rock composition, texture

and structure and, therefore, it is difficult to

relate them to former still stands of sea level,

Purthermore, such a correlation is almost

impossible anyway, because modern sea level

around Australia is believed to be within a

metre or so of its former level during the late

Pleistocene (Hails 1968; Chappell 1976).

The problem of dating Pleistocene sea levels

in coral reef areas has been outlined by Chap-

pel er al, (1974). In addition, many C!* dates

' Centre for Environomental Studies, University of

+ Department of Geology, University of Adelaide.

‘eported from Pleistocene strandlines near

present sea level have proved to be unreliable,

and therefore other dating methods must be

used before an accurate reconstruction of past

events can be undertaken (Thom 1973),

Because of these facts, it is now generally

recognised by researchers conducting process

studies in the coastal zone that depositional

features, such us barrier beaches containing

diagnostic fossils, datable organic material and

soil horizons, are better indicators of relative

changes in mean sea level.

During a recent survey of the coast of upper

Spencer Gulf, as part of a detailed study of the

submarine geology and nearshore processes

within the region, the writers traced well

preserved stranded shingle beach deposits from

Black Point, 15 km northeast of Whyalla,

northwards along the shoreline to a point

opposite Snapper Point 8 km south of Port

Augusta, a distance of about 50 km (Fig. 1).

The term ‘shingle’ is used here to describe

beach gravels composed predominantly of

pebbles and cobbles.

Adelaide, North Tce. Adelaide, S. Aust. 5000.

V7) J. R, HAILS & V, A, GOSTIN

Py AUGUSTA

‘|

uw j

we Ape ome y

arts

Blanche

= Horbor

we pievent sliieane

PONISI URIED mbureline ts

ant figh chant af oem feyel

SPENCER

GULF

“eee Deelian ol Siiwnoed int

Hoacl® depute

® cectine oi Hanguert of

Marenal COMA uty Shanded

beech deposit

mm fenorh of waive TEPeh gun

gee level

@ownges lereh

Pig. I. Generalized mip of upper Spencer Gulf

to show distribution of stranded beach

deposits and maximum fetches during a

-++-3 mehigh stand of Pleistocene sea level.

The purpose of this paper is to describe

brielly the main diagnostic features of these

deposits und to consider the conditions under

which they may have been emplaced during a

Pleistocene high stand of sea level. As far as

the writers ure aware, these deposits have only

been recorded on the Cultana (1:63360)

geological may, and in the Black Point—Point

Lowly area by Crawford (1963) who de-

scribed them a§ Quaternary ‘emerged offshore

burs’ lectonically elevated to their present

position. However. Firman (1965), without

ciling Crawford's earlier work, mentions a

}0-ft Tertiary-Quaternary high stand of sea

level and associated uravel beach ridges.

Stranded beach deposits

Most of the stranded beach deposits form

sinuous, fit-topped ridges which stand 3-5 m

above (Meal sea level (Fig. 2A). They are

usually narrow, no more than LO-15 m wide,

although at one locality, 15 km south of Port

Augusta, one ridge ts more than 75 mon width

(Figs 2E and 2F), The seaward slope of these

ridges Usually exceeds 30°, which is generally

steeper than the landward or lee slope. The

75 m-wide ridge shown in Figs 26 and 2F has

mo extremely gentle lee slope and resembles a

Washover fan, a feature deposited on a coast

during hurricanes and cyclones when beach

ridges are extensively eroded by storm waves.

In some localitics the shingle deposits form

clills behind the modern beach. An intervening

narrow ‘flat’ between the cliffs and the back-

shore is now used as a toad for vehicular

traffic, particularly between Port Augusta and

Rlunche Harbour. Many ridges are vegetated

With low scrub, but this is generally absent

fram the flat, crestal surfaces because of the

extreme permeability of the gravels,

Rounded to sub-angular pebbles and cobbles

of Precumbrian sandstones and quartzites are

the main constituents af the ridges (Fig. 2B)

These have been derived from either alluvial

fans, dissected by ephemeral Streams, or

colluvium that mantles neighbouring cliffs

usually cut in bedrock, A few of the cliffs,

though, comprise remnant alluvial-lan deposits,

In the Point Lowly area the shingle comprising

the ridges iy significantly more rounded than

that on most other beaches where the material

has been derived directly from cliffs and our

crops of Precambrian bedrock.

At most localities the stranded shingle ts

moderately sorted and varies in size from large

flat cobbles, as in the Black Point-Point Lowly

sector, Lo more ubiquitous sub-rounded, small

cobbles and pebbles elsewhere ulony the Gulf

coust. Some lateral reduction in mean clast

size hax heen noted away from source areas,

but the glongshore movement of gravel has

been minimal, as evidenced by the absence of

recurved spits,

The thick-shelled estuarine cockle Anadare

frapezia 18 woundant in the relict beach deposits

especially in Fitzgerald Bay and the northern-

most part of the Gulf (Figs 2C and 2D).

According to Gill (1977), this species migrated

to Australia during the Pleistocene epoch,

probably more than 400,000 years age. and

became abundant in southern Australia during

the Last Interglacial. However, A. trapesia is

absent from the modern sediments of South

Australia except where it has been reworked

trom Pleistocene deposits. The shells found in

the stranded shingle ridges are entire, non-

abraded valves und therefore do net appear to

have been reworked from early Pleistocene

tlepasits-

STRANDED SHINGLE BEACH RIDGES, UPPER SPENCER GULF 171

Fig. 2A Stranded sinuous shingle beach ridge, looking north, Fitzgerald Bay. (Map Ref.

tana 6432-IIT, 1:50 000).

pn hag. :

Dae

568534, Cul-

a “ F =

Fig. 2B. Cobbles and scattered boulders comprising 3m beach ridge, Stony Point. View looking east

towards Point Lowly. (Map Ref. 575456, Mambray 6432-IT, 1:50 000).

Fig. 2C. Road cut through stranded shingle beach, containing abundant shells of Anadara trapezia,

Saints Bay. (Map Ref. 580825, Davenport 6432-I, 1:50 000).

Fig. 2D. Part of road-cut in Fig. 2C showing in situ Anadara trapezia.

Fig. 2E. Landward margin of non-vegetated part of washover fan shown in Fig. 2F, and located 15 km

south of Port Augusta. (Map Ref. 586865, Davenport 6432-1, 1:50 000).

Fig. 2F.

Discussion

No marine gravels have been located above

the Pleistocene shoreline reported here, and

very little gravel has been recovered in 3-5 m

long, undisturbed vibrocores obtained from the

seabed immediately offshore from the stranded

shingle beach ridges. Therefore, it may be

View looking north showing washover fan with road on seaward side. Location as in Fig. 2E.

inferred that there has never been a substantial

offshore reservoir of shingle in upper Spencer

Gulf. Also, the fact that the shingle ridges dis-

play minimal grading, and no marked variation

in width in an alongshore direction, suggests

that there has been only minor northerly or

southerly movement of beach material along

the embayed western shore of the Gulf in the

past. The shingle has been derived from either

outcrops of Precanibriah quartzite or, more

commonly, adjacent dissected alluvial fans

which, as stated previously, form cliffs in some

localities. It appears thal the shingle was moved

a short distance offshore, abraded in the wear

shore zone and wltimately deposited as beach

ridve maternal. In the relatively confined and

sheltered parts of northern Spenver Gull

today, the movement of beach gravel ts some

whut restricted within the inter-tidal zone by

the mangrove Avicennia marina var, resinifera

((Forst f,) Bakh vd, Brink 1921) which

urows on suh-angular sandy gravel und often

hetween blocks of cemented Pleistocene con-

glomerate.

If Gills thesis on the migration of Aiddara

trapezia 18 correct the stranded beach ridves

Which contain 4, trapezia could have heen

built during cither the Last Interglicial

(120,000 years BP) or during 4 late Pleistocene

iNterstadhal, about 30,000 years BP because, as

stuled above, there is no evidence of an earlier

Pleistocene sea level in upper Spencer Gulf

The presence of entire and unweathered shells,

the well-preserved beach ridge surfaces, and the

lack of fine windblown sediment on the ridge

lops collectively suggest.a very Jute Pleistocene

age, but dating is obviously needed to establish

an absolute age.

Regardless of the age of the stranded beach

nudges, their presence is significant in determin-

ing past wave and wind régimes in the northem

part of the Gulf. In this context, it is pertinent

to consider the fuctors involved in the forma-

tion of such ridges. I) the afea of generation,

ihe height of sea waves and their period are

functiuns of the duration that the wind (starm)

blows (DB), the wind velocity (U1), and the

length of fetch (F) or the distance over which

the wind blows, The feteh length is a major

factor because it determines not only the time

during which wind cnergy is trunsterred to (he

sea suriuce, but also the wave height (MH) and

period (1). ‘Thus, for relatively short fetches,

waves depend upon the fetch lensth (F) und

willl velocity (WU), and foe long fetches on

wind velocily and duration (D). This relatton-

ship can be writen svinbetically us

H,) -—f (UB).

It can be seen in Figure 1 that winds would

have been muily southeasterly in order to

build most of the shingle ridges hecause smaller

wives arc penerated from other dueetions.

Even if easterly winds occurred less frequently

J. RK. HAILS & V, A. GOSTIN

than dil others they were, nevertheless, the

dominant wilds that eeneraled waves able to

move shingle aud form beach ridyes. Fine sand

and mud could haye been inovest selectively

by Currents and carried olonyshore in suspen-

sion. tt is ulso known that variation in wave

energy is partly responsible for variations m

particle size parallel to the shoreline and that

luryer particles ure associated ‘with greater

energy. Theoretically, wave heights of about

3-5 m above mean sea level can be peneraced

hy winds of 50 knots blowing over » fetch of

4) km—one which far exceeds Uose in upper

Spencer Gulf today—bue waves of this height

are usually destructive.

On the other hand, shingle can be deposited

a few metres ubave » given datum by constiruc-

tive swell and, in the light of this fact, it

should he considered whether ar wot the

stranded nudges were emplaced during a +3 m,

or slightly Jower, stillstand of the sea during

the Pleistocene. Certvinly, the 2 m ditference

in the maximum heipht of ridve crests reported

here could reflect degree of exposure to, and

varivlions in, wave eoegy as determined by the

length nf fewh in the past, and coastal con-

figuration,

The present tidal range in the Gulf is ubout

2 m, but Raduk & Raupach (1977) have

shown in recent studies thal weather systems

raise mean sea level avsinst the south coast of

Australia because of barometric pressure and

wind stress operating ever large areas of the

Southern Ocean, Waves and tides, in durn, wre

superimposed on this mean sea level, Because

changes if (ean seu level are relatively slow,

they are able to penetrate into confined water

budies like Spencer Gulf ind Gulf St Vincent

i South Australia, aml may consequently

indice notable water exchange und sediment

wiovement. Coastal eraston slong the soubhern

margin of Australia today vat, in laet. he

linked to these variations. LF similar meteoro-

logical conditions existed in the late Pleisto-

cene, and asobaric pressure gradients were

steeper, there is little doubt that shingle ridges

could also have been constructed us a result of

higher Wave cnergy in upper Spencer Gulf,

His worth mentioning that studies by VYeeh

(1966) tn the Central Pacific have shown that

sea level stood approximately 2-6 m above

nidern datum during the Last taterglacial.

However. wide-scale correlations can be $us-

pect because of reyionyl and Jocul Eaetors, some

of which have been discussed Here with reewrd

(o South Australia,

STRANDED SHINGLE BEACH RIDGES. UPPER SPENCER GULF 173

As only a small area of the Gulf is under

review in this paper the writers cannot debate

with justification whether the ridges have been

elevated as a result of tectonic activity as pro-

posed for the Black Point-Lowly Point area

by Crawford (1963), Although tectonism

cannot be ignored on a much larger regional

scale it seems unlikely, for the reasons just

cited, that it can exclusively account for the

3-5 m heach ridges.

In conclusion available evidence indicates

that the stranded shingle ridges in upper Spen-

cer Gulf are Pleistocene in age, and were most

likely built during a +3 m high stand of sea

level when easterly winds predominated in the

reyion and large waves from the southeast

dissipated their edges along the western shore.

No corresponding shingle ridges are known

along the eastern counterpart of the Gulf de-

spite the fact that southwesterly waves travel

across the longest fetch today.

Acknowledgement

The writers wish to acknowledge the support

of an ARGC grant for the detailed study of

Spencer Gulf which is currently in progress.

References

CuHarekyi, J. (1976) Aspects of late Quarternary

palueogeography of the Australian-East

Indonesian Region. /n Kirk, R. L, & Thorne,

A. G. (cds.), “The Origin of the Australians”,

{1-22 (Human Biology Series No. 6, Aus-

tralian Institute of Aboriginal Studies, Can-

berra; Humanities Press, New Jersey).

CHAPPELL, J., BROECKER, W. 8,, Potacu, H. A, &

Thom, B. G. (1974) Problem of dating Upper

Pleistocene sea levels from coral reef areas.

In “Proceedings of the Second International

Coral Reef Symposium" 2. 563-571 (Great

Barrier Reef Committee, Brisbane, December

1974).

Cook, P. J.. Cotwetr, J. B., FirnMayn, J. By,

Linpsay, J, M,, Scwwerner, D, A. & Von

per Borcu, C, C. (1977) The Late Cainozoaic

sequence of southeast South Australia and

Pleistocene sea-level changes. Bur. Min. Res.

J, Geol Geopliys. 2, 81-8%,

Crawrorp, A. R. (1963) Quaternary sedimentary

breccias and cmerged offshore bars near Point

Lowly. Quari. geol. Notes, geal. Surv. 8,

Atist. 5, 1-2.

Firman, J. B. (1965) Late Cainozoic se¢dimenta-

tion in northern Spencer Gulf, South Anus-

tralia, Trans, R, Sec. 8S. Aust. 89, 125-131,

Git, BE. D. (1977) Time of migration of the

mollusc Anadara to SE Australia. Search 8

(1-2), 40-41,

Git, E. D. & Amin, B, S. (1975) Interpretation

of 7.5 and 4 meter Last Interglacial shore

platforms in southeast Australia. Ihid. 6(9),

394-396,

Hats, J. R. (1965) A critical review of sea level

changes in Eastern Australia since the Last

Glacial. Aust, Geogr. Stud. 3, 63-78.

Hats, J. R. (1968) The Late Quaternary history

of part of the Mid-North Coast New South

Wales, Australia. Trans. Inst. Brit, Geogr. 44,

1059-1069,

Rapok, R. & Rauracn, M. (1977) Sea level and

transport phenomena in St, Vincent Gulf.

Jnst. Engrs 3rd Aust. Conf. Coastal Ocean

Eng, 103-109,

TuHom, B. G., Haws, J. R., & Martin, A. R. H,

(1969) Radiocarbon evidence against higher

Postglacial sea levels in eastern Australia.

Marine Geol, 7(2), 161-168.

Tuom, B. G. (1973) The dilema of high inter-

stadial sca levels during the last glaciation:

Pragr. Geogr. 5, 170-245.

THom, B. G, & CHAPPELL, J, (1975) Holocene

sea levels relative ta Australia, Search 6(3),

90-93.

Veen, H, H. (1966) Th®*?/U288 and Us /Uss

Ages of Pleistacene high sea level stand,

J, Geophys, Res. T1, 3379-3386.

VOL. 102, PARTS 7 & 8 30 NOVEMBER, 1978

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

McKenzie, K. G. Ostracoda (Crustacea: Podocopida) from southern Australian

salt lakes, with the description of Reticypris new genus - - 175

Parker, §. A. & Cox, J. B. Notes on the birds of Pearson, Dorothee and Greenly

Islands, South Australia - - - - - - 191

Flint, D. J. Deep sea fan sedimentation of the Kanmantoo Group,

Kangaroo. Island - - - - - - - - 203

Mawson, Patricia M. A new genus Adelonema (Nematoda: Oxyuridae) from

Australian phalangerid marsupials - - - - - 223

Annual Report of Council - - - - - - - - - ei APA)

Award of the Sir Joseph Verco Medal - - - - - - - - 228

Balance Sheet - - - - - - - - - - - --— 229

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

OSTRACOD (CRUSTACEA: PODOCOPIDA) FROM SOUTHERN

AUSTRALIAN SALT LAKES, WITH THE DESCRIPTION OF RETICYPRIS

NEW GENUS

BY K. G. MCKENZIE

Summary

Ostracoda are idntified from collections made in South Australian and Western Australian salt

lakes. The new genus, Reticypris, new species Cyprinotus edwardi, Diacypris paracompacta, D.

occidentalis, Reticypris herbsti, R. dedeckkeri, Cyprideis westraliensis, ?Microcytherura difficilis,

Cytheroma sudaustralis and new subspecies Mytilocypris tasmanica chapmani are described.

OSTRACODA (CRUSTACEA: PODOCOPIDA) FROM SOUTHERN

AUSTRALIAN SALT LAKES, WITH THE DESCRIPTION OF

RETICYPRIS NEW GENUS

by K. G, McKENZIE*

Summary

McKenzir, K, G. (1978) Ostracoda (Crustacea: Podocopida) from southern Australian salt

lakes, With the description of Reticypris new genus. Trans, R, Soe. S. Aust, 10207),

175-190, 30 November, 1978,

Ostracoda are

identified from collections made

in South Australian and Western

Australian sult lakes. The new genus, Reticypris, new species Cyprinotas edwardi, Diaeypris

paracoimnpacta, D, occidentalis, Retieypris herbsti, R.

dedeckkeri, Cyprideis westraliensis,

*Micracylherura difficilis, Cyvtherome sudausiralix and new subspecies Mytilocypris tasmanica

chapmani are described,

Introduction

The continental Ostracoda of Australia are

gradually becoming better known, thanks to

the impetus given to taxonomic studies by

limnologists. For an arid continent the study

of saline lake environments has obvious rele-

vance and, since Ostracoda are one of the

commoner groups in such environments, it is

regrettable that little relevant taxonomic work

has heen undertaken. The opportunity to

improve this situation came with an invitation

from W, D, Williams to study the ostracodes

in saline lake collections made by him in

southern South Australia and Western Aus-

tralia in 1971 and 1972, The chemical com-

position of these environments and detuiled

locality maps are provided in Williams &

Buckney (1976),

Previously, the large endemic species have

been studied by De Deckker (1974, 1975,

1976) and MeKenzie (1966), and yaluable

work was done by Herbst (1957, 1958) on the

endemic genera Platyeypris and Diacypris. In

addition to species described by these workers,

u new genus, eight new species and a new sub-

species were identified in the course of the

present study.

Materials and methods

Soft parts have been drawn using a Wild

M.20 camera lucida. External carapace mor-

phology was photographed by scanning elec-

tron microscopy but internal features have

been drawn,

The German taxonomic terms Zahnborsten

and Strahlen are used commonly in the general

ostracode literature, Zahnborsten are spine-like

bristles on the maxillule third lobe which are

often barbed. Strahlen are pilose setae on the

respiratory epipods of the mandible, maxillulue

and maxilla (P 1). The terms P I, PU, PII

refer to paired thoracic limbs on the rear of

the body. The a, 8, and y sensory bristles on

the mandible cndopod were defined and illus-

trated in McKenzie (1977a),

The conventions: L = length, H = height;

B = breadth; RV = right valve; LV = left

valve; have been used throughout, The term

“population” means at least » dozen indivi-

duals of a species, including adult males and

females and juveniles.

Types are stored at the Australian Museum,

Sydney and the remuinder of the material has

heen returned to W, D. Williams, University

of Adelaide, Copics of appendices which give

locality details (Appendix I), ostracode deter-

minations and numbers of specimens by loca-

lity (Appendix IT), and associated fauna

(Appendix TIl) may be obtained from the

author.

" Riverina College of Advanced Education, Wagga Wagga, N.S.W.. 2650.

176

Systematic descriptions

Superfamily: CYTHERACEA Buird, 1850

Family: CYTHERIDEIDAE Sars, 1925

Subfamily: CYTHERLDEINAE Sars, 1925

Genus: CYPRIDEIS Jones. 1857

Cyprideis westraliensis sp, nov

FIGS 1-3, 21-28

Holotype: AM P26650, adult male,

Peraryyess AM P26651, 2 adult females, |

adult male,

Type locality: Causeway at Luke Preston, WA

Material: Populations from Lakes Preston and

Coolongup, WA.

Deseriptien:; Shell Whitish, but appearing

brawaish because of yellaw-brown soft body

inside} medium sized; elongate subrectangular

in lateral views mequivalyed with LV distinctly

larger, and RY possessing small posteroventral

spine in some individuals; ornamented with

large shallow pittings: dorsum straight, slightly

inclined posteriorly; anterior more broadly

rounded than posterior; venter weakly inflexed

anteriomedially; greatest height just in front

of ventral muscle soars, wnd about half length,

Th dorsal view subelliptical: tapering anteriorly,

rounded posteriorly; displaying sex — di-

morphism: females broadened posteriorly

wheress males are not; greatest breadth medial

and under half length in males, but postero-

medial and about half length of females, In-

ternally: lamellae moderately broad: narrow

anterior and posterior vestibules present, inner

margia regular) marginal pore canals numer-

ous, fen branched; normal pore canals scat-

tered, sieve type; central muscle scars com-

prising 4 adductors in subvertical row, « large

V-shaped frontal scar, a fulcral scar and at

least one large mandibular, some dorsal scars

observed also. hinge entomodont, consisting in

K. G, McKENZIE

RV of elongate, disiinetly crenulate terminal

tooth-like projections, and medially with crenu-

Jate furrow anteriorly which becomes weakly

crenulute ridge posteriorly; LV comple-

mentary,

Antennule robust, S-scamented) segmental

length ratios 25:22:10; 10011; armature com-

prising mainly strong claw-like spines, lermunal

segment aboul 34 times us Jong as wide, An-

(enna powerful, 4-segmented; segmental Jength

tatios 35:7:33:5; armatyre normal; flagellum

long, Z-seemented, Mandible coxa powerful;

coxal teeth decreasing regularly io size trom

front to rear; endopod normal; ¢pipod with 5

Strablen.. Maxillule palp and lobes normal; epi-

pod with 17 Strahlen, including one which

points downwards, Thoracic limbs (P 1 to P

TEL) all functioning as walking legs, and dis-

iying asymmetry between right and left

imbs, especially in male P U, which js typical

for this genus. Brush shaped organs present in

male. Purca much reduced. Posterior of female

body flattened abd produced into a pointed

lobe. Cups of nauplius eye fused, Hemipenes

Jarge, comprising an ovate posterior girdle

strengthened by humerous muscle bands, pnd

acuminale anterior lappet; this combination

typical for genus. Natural colour of soft body

yellow-brown.

Dimensions: Holotype, adult male—L. ~~ 0,90

oun, H = 0.44 mm, B — 0.44 mm, Paratype.

B ~ 1.46 mm.

Divscussion: The genus Cyprideis is well Known,

not only because i is polyhuline and regularly

encountered i a Variety of fresh, brackish and

saline environments, but also because its dis-

tribution is cosmopolitan, extending tu every

continent except Antarctica, Long piyo it was

hypothesised that this cosmapolitan distribu-

tion Was effected by birds, and some recent

Pigs 1-20. Figs L-3: Cyprideis westrulionsis sp. nov.. holotype. 1: external LV, 4 40; 2: external RV,

« 455 32 sieve type normal pore canal, x 1500, Fig, 4. ? Microcytherura difficiliy sp. Nov..

holotype, external RV, x IML Fig. 5, Linnweytlere mowhrayensis, female, external RV. 4

100, Fig. 6, Mytiloeypriy tasmanica ehapniani ssp. nov.. holotype, internal RV,» 15. Fig.

7, Diacypriy occidentalis sp, fov, paratype AM P26674, detail muscle scars internal RV

x 373; Pigs 8-10: Cyprinotus edward: 3p. Nov. &, paratype, AM P26664, internal RV_ 4s

25; Fig, 9, holotype, male. external RV, 4 25; Fig. 10, timed simple normal pore canal

of holutype » 800. Figs 11, 12: Diaeypris paraconipacta sp. nov, puralype, AM P26670,

female. 11! external LV. x 60) 12) external RV. « GO. Figs 13-14: Diacypris eeciden|alis

sp, pov. paratype, AM P2667d, female. 13: internal RV. ¥ G5; 14) external LV, s S55

Fig. 15, Relicvpris herhsti gen, nov. sp. nov,, holotype. mule. external LY, » 60, Fig 16,

9 Microcytherura difficilis sp. voV. holotype, dorsal view x 110. Fig. 17. Retieypris herhsti

en, Mov, sp. nov, Holelypes rimmed simple normal pore canals, x 300. Plas 18, 19:

Reney pets

x fOs DY: external LV, x Al, Pie,

femiile. rimmed, simple, tormal pore cana

dederkkerl gen. WV. by. nev., pamilype, AM P2662. lemale [8 dorsal view.

0, Divevpels oeridentaldy sp. nev. purutipe AM P2674,

% 440.

T LAKE OSTRACODA

AUSTRALIAN SAL

178 K. G. McKENZIE

Figs 21-26. Cyprideiy westraliensis sp. nov, holo-

type, male; 2l; antenna; 22: distal

P Uy 23: distal P Mi, 24; P & 25:

antennole; 26; hemipenis. All magni-

fications x 300,

eXperimental confirmation has been obtained

(Léffler & Leibetseder 1965), Because Cypri-

deis broods its first instar im the shell, the

passive transport of both sexes or of tmpreg-

nated or brooding females is necessary to effect

distribution across barriers such as the oceans

ant great deserts (McKenzie 1973),

Over 30 species of Cyprideiy have heen

described but, because the carapace morpho-

logy can vary intraspecifically and 1s similar tn

practically all species, distinctions often rest

on differences in the male hemipenis, which

follows u pattern characteristic of the genus,

However, the hemipemis of Cyprideis westra-

Jiensis, in particular the morphology of the

imternal chitinised process, is not matched in

any previously described species.

Derivation of name: Fram Western Australi,

Family: CYTHBROMATIDAE Elofson, 1939

Subfamilys CYTHEROMATINAE Elofsan,

1939

Genus! CYTHEROMA Miller, 1894

Cytheroma sudaustralis sp. ooy.

FIGS 30, 35-42

Holotype: AM P26652, adult male.

Paratypes: AM P26633-26654, 2

females, 1 adult male.

Type locality; Coastal pond between Port Clin-

con and Wakefield, S.A.

Material: Five topotypic adults

Description: Shell whitish; medium sized;

elongate subreniform in lateral view; incqui-

valved, left valve (LV) slightly larger than

right valve (RV) and overlapping it ventrally;

shell smooth; dorsum gently convex; anterior

rounded; posterior broadly rounded; venter

weakly inflexed anteromedially; greatest height

just behind addactor muscle scars, and about

half length. In dorsal view regularly elliptical;

greatest breadth medial and about half length,

Internally: lamellae broad; line of coneres-

cence marginal; anterior vestibule large, pos-

terior vestibule large and elongate: inner mar

gin regular; marginal pore canals short and

numerous; normal pore canals large, sieve-

type, numerous; central muscle scars compris-

ing 4 adductors in subvertical series, plus

broadly V-shaped frontal scar, fulcral scar, and

two mandibular scars; hinge very weakly

lophodont, RV with jobate anterior antislip

projection and low weakly crenulated posterior

projection, LV with complementary antislip

projection, weakly developed median bar and

shallow posterior groove.

Antennule 6-segmented; segmental length

fatios 7:7:2:1,5:2,5:3; armature consisting

mainly of strong claw-like spines; terminal sez-

ment about 5 times as long as wide. Antenna

broad and short; segmental Jength ratios

9:11:4; armature normal; flagellum 2-seg-

mented; antennal gland lobate, Mandible coxa

normul, second tooth from anterior slightly

more prominent than others which otherwise

diminish in strength regularly from front to

rears endopod normal; epipod with 2 very long

Strahlen and | or 2 shorter Strahlen. Maxillule

palp and lobes normal; epipod with a single

aberrant Strahl] and 14 feathered Strahlen,

Theracic hmbs normal, increasing in size from

P ito P TIT as illustrated. Posterior of body

hirsute in hoth sexes, Cups of the nauplits eye

fused.

Carapate sex dimorphism very weak,

females slightly larger and broader than males,

Hemipenes large, about 40% of body length,

pointed anteriorly and similar to those iflus-

adult

AUSTRALIAN SALT LAKE OSTRACODA 7

irated for other cytheromatids, being charac-

lerised by prominent penifera,

Dimensions: Holotype, adult male—L = ().53

mm, H = 0,26 mm; B = 0.27 mm. Paratype,

adull female—L > 056 mm: H = 0.28 mo

B= 0.29 mm.

Discussion: Cytheroma has heen described

rarcly in the literature. Hartmann (1964) notes

five species, of whieh C_. similiy Skogsberg,

1959 js probably a Parwcyrherome, and

Schornikov (1969) has described a sixth,

Further, Species DC) Muddocks, 1966 may be

a Cytheroma. These other species all differ in

shape from the new species,

The distributions of other yenera im the

family form an interesting biogeographic pat-

tern, Paraeytheroma Juday, 1907 und Mega-

eyihere Purl, 1960 (which some authors have

synonymised) oceur in the Caribbean and on

both coasts of the Americas as far south as

Valdivia, Chile (Hartmann 1962). Panto-

eviheroma Marinov, 1960 is restricted to the

Black and Avoy Seas (Schornikov 196%). The

other Cytherome species oecur in the North

Atlantic, Mediterrancon and Red Sea, possibly

even to Madugasear (Maddocks 1966), There

um no secords of these penera from the

southern coasts of Africa (Hartmann 1974),

Cytherama sudaustralis therefore may be

considered as a palimpsest of an earlier

Tethyan distribution pattern, once continuous

for many groups from the Gulf af Mexico to

Australasia (Ekman 1953, McKenzie 1967b).

Perivation of name: Fram South Australia.

Family; CYTHERURIDAE Miiller, 1894

Subfamily: CY PTHERURIDAE Miiller, 1894

Genus: MICROCYTHERURA Miller, 1894

2 Microcytheruva difficilis sp. nov.

FIGS 4, 16, 34, 43-51

Holotype; AM P2G655, adult mile,

Paralypes: AM P26656-26657, population of

males, females und juveniles

Type lecnlity. The Coorong, opposite Mount

Mills, S.A.

Material; A topotypic popularian,

Deseriprlon, Shell whinshy small subrect-

angular in lateral view; equivalyved; weakly

reliculate over entire sutfaec. seliculations

forming concentric putter anteriorly and ven-

trally; dorsum straht; anterior rounded,

trending anteroventrally: posterior rounded:

Venter Weakly iiflexed anteromedially; greatest

height slightly in front of muscle seurs and

about helf length, In dorsal view, elliptical;

narrowing antenorly, but more rounded pos-

teriorly; greatest breadth medial, aud just over

half Jeneth. Internally: Jamellae moderately

broad: wnterior Vestibule and small posterior

vestibule present; marginal pore canals num-

ber about I) gnteriorly and 5 ventrally, all

Short and straight; normal pore canals scat-

tered, sieve type: central musele scar pattern

consisting of subvertical row of 4 wdduetars, a

V-shaped frontal sear and 2 mandibulars,

hinge merodont, comprising terminal crenulate

teeth in RV with intervening furrow and ter-

ininal crenulote sockets in LY with an inter

vening ridge. Shell sex dimorphism not

marked, hut females tend to be shorter and

relatively broader than mates.

Anteonule 6-segmented: segmental length

ratios 14:17'°5:5:6:8; terminal segment about

4 times as long as wide) armature less powerltl

than in Cyprideis and Cytheroma. Antenna

4-segmented; segmental Jenyth ratios 13:5:

26:3; flagellum extending to about Lip of ter-

minal claw and bent distally: terminal elaw

short and stout, Forelip denticulate distally,

Mandible coxa with anterior tooth projecting

distinctly forwards of others (typieal for this

venus); endopod normal, segments relatively

wide, Maxillule partially destroyed during dis-

seghion, comprising an epipod with ubout 10

Strohlen and a normal palp and lobes; length

ratio of 2 palp segments 13/4. Walking legs

(P J to P WV) increasing in length from PT

to P UT. Hemipenis (Fig, 51) comprising a

large posterior part and small pointed anterior

lappet.

Dimensions: Holotype, adult male—L — 0,37

mm, H = 0.21 mm, B= 0.20 mm, Paratype,

adult fernale—L = 0.35 mm: = 0.20 mm,

B= 1.20 mm.

Discussion. This species proved to be a taxo-

nomic problem, being like Microcythernra in

curapace characters except that the posterior

cauda, which is weakly expressed in the

European species of the venus, appears to be

absent or almost uhsent in this species. But the

Australasian getlus Loreeyrhere Hornibrook,

1952 1s also simular mm carapace characlers, As

faras the sofl parts ance concerned, this species

has the prolonged anterior tooth on the man-

dible coxa which charaeterises Mieroevrhertira,

and the typical antennal flagellum and slender

antennule of cytherurines, but the walking legs

are Jess slender than in cytherurines and the

hemipenis only vaguely resembles the Micro-

evtherura patiern (Sars. 1926, description of

kK. G. McKENZIE

180

AUSTRALIAN SALT LAKE OSTRACODA 18)

M. fulva), On balance, the difficulties jn mak-

ing a confident generic placement remain.

This taxon is distinct from two previously

described Australian species assigned to the

genus (McKenzie 19674) of Which ane, M,

riebeli, is confirmed in the genus on soft parts

as wel] (McKenzie, unpublished data),

As a generalisation, most of the difficulties

in the taxonomy of such ostracodes stem from

their small size and the need to dissect a

minwte body from the small carapace hefore

examining it further. Often, critical details are

destroyed as a result,

Derivation of name: From Latin: difficilis =

difficult.

Family: LIMNOCYTHERIDAE Klie, 1938

Sublamily: LIMNOCYTHERINAE Klie,

1938

Genus: LIMNOCYTHERE Brady, 1868

Liuimocythere mowbrayensis Chapman, 1914

FIGS 5, 32

Lininteythere {si¢) mowbrayensis Chapman,

1914

Linmicythere (sic) steida Chapman, 1919

Limnicythere (sic) percivali Brehm, 1939

Limnteythere (sic) mawhravensix: Hornibrook,

1955

Locality: Lake Coolongup, W.A,

Family: CYPRIDIDAE Baird, [835

Subfamily: MEGALOCYPRIDINAE Rome,

1965

‘Tnhe! MYTILOCYPRIDINI De Deckker,

1975

Genus: MYTILOCYPRIS MeKenzie, 1966

Mytilocypris tasmanies McKenzic, 1966

Localities: Several in W.A,, from Lake

Walungup to a fake near Lort River (see

Appendix IT).

Mytilocypris tasmanica chapmani subsp. nov-

FIG. 6

Holetyper AM P26659, adult male.

Paratype: AM P26660, adult female.

Type locality Lake Coolongup, W.A.

Matérial: A topotypic population ++ 5 indivi-

duals From W.A.

Description; Shell whitish-yellowish, large;

acutely subtriangular (myliliform) in lateral

view; equivalyed; smooth; dorsum straight and

inclined towards rear; anterior broadly

rounded; posterior broadly acuminate; venter

weakly jnflexed anteromedially; greatest height

anteromedial and slightly less than half length.

Jn dorsal view subelliptical, narrowing at both

extremities; greatest breadth medial and about

2/5 length, Tnternally: lamellae broad

anteriorly amd posteriorly, narrow ventrally;

line of concrescence submarginal: immer margin

regular; marginal pore canals numerous and

straight; normal pore canals scattered, simple,

open; central muscle scars a rosette of 4-6

adductors plus 2 mandibulars and small frontal

sear, hinge of usual ridge and groove type.

The soft body is like that of Mylilocypris

tasmanica but the male of ehapmant differs at

least in that ft has only about 50 rosettes on

the Zenkers Organ (about 60 in tasnanica),

The hemipenis, however, is not very different.

Other well marked differences are in the shell

proportions, with chapmaii being higher with

respect to its length than fasmmanica, In addi-

tion, these characters have not been reported

previously for the genus but are likely to be

constant at the generic level; rake-like organs

with 9-10 teeth, one bifid; mandible endopod

ventral a bristle long and slender, ventral 8

bristle pilose, shorter and stout, distal y bristle

thick and tapering with spiky hairs distally,

Dimensions: Holotype, adult male—L — 2.68

mm, H = 1.25 mm, B = 1,10 mm. Paratype,

adult female—L = 2.48 mm, H = 1.45 mm,

B = 1,33 mm,

Discussion: The taxon ts described as only a

subspecies because although it dilfers in several

Catapace and soft part characters, the hemi-

penis is clasely similar to that of the nominate

subspecies, Tf appears to differ sufficiently from

ather species in the genus described by Chap-

mah (1966) and De Deckker (1978) to sus-

tain a new taxon; in particular because the

Figs 27-34.

anteser, 28: inlertal

Pigs 27, 28) Cyprideis westraliensis n, sp. paratype, AM P26651, female, 27) internal LV

RY posterior,

with posteroventral spine, % Fig. 29,

Cyprinetus edwardi sp. nov., paratype, AM P26664, female, mandible endopod, detail +

bristle, ¥ 400. Fie. 30, Cytherema sudaustralis sp. nov., holotype, male, internal LV, x

150, Fig. 31, Diaevpris paracompacta sp. nov., paratype, AM P26672, male, internal LV,

» 150.

Pip. 32, Limmnoevthers mawhravensis Chapman 1Y1l4, AM P26658, female, internal

RV. « ISA. Fiz. 33, Rerleypris fherbsti gen, nov., sp. nov. paratype, AM F26678, female,

infernal EV % 150, Fig, 34, 7 Microeviherura difficilis sp. nov., holotype. male, internal

RY, & 150,

1$2 K. G. MCKENZIE

valve proportions (length:height) are unlike

those in the other species, Sympatry with the

nominate subspecies does not occur, but since

Ostracoda are readily transported by birds and

other agencies (McKengse 1973) it cannot be

ruled out as a future possibility, in which case

the resulting introgressions should make an

interesting slody.

Derivation of name: For M.A, Chapman who

described several large Australian species.

Genus: AUSTRALOCYPRIS De Deckker,

1974

Australocypris bypersalina De Deckker, 1974

Localities; Eleven localities in S.A. and WA

(see Appendix IT); the commonest species ip

the collection.

Anstralocypris robusta De Deckker, 1974

Locality; Moderately lony, shallow jake 45 kow

N of Kingston, S.A.

Subfamily; PLATYCYPRIDINARF. Hartmann

& Puri, 1974

Genus. PLATYCYPRIS Herhst, 1957

Platycypris bauerl Herbst, 1957

Localities: Several localities in S.A, and W.A,

(see Appendix 1).

Subfainily: CYPRINOTINAE Bronstein, 1947

Genus: CYPRINOTUS Brady, 1886

Cyprinotus edwardi sp. nov-

FIGS 8-10, 29, 52-57

Holotype: AM P26663, adule male.

Pararypes: AM P26664, adult female and three

adult mules,

Type locality; Wagin Lake, W.A,

Material: Nine topotypic adults.

Deseriprion: Sheil yellowish to brownish, large:

subtrapezoidal in lateral view: murkedly t-

equivalved, RV overlipping LV by a promin-

ent dorsal hump, LV larger without any dorsal

hump but overlapping KV anteriorly und ven-

trally. shell punctate except i muscle scar

region; dorsum straight and inclined pos-

teriarly in LV, hump-like in RV; anterior

rounded, pointing anteroventrally; posterior

more broadly rounded; Venter inflexed

medially, ventral margin of RY denticulate

anteriorly and posteriorly; greatest height just

behind muscle scars and 8/58 of length in RV

but about half length in LV. In dorsal view

somewhat flexuous; hump turning outwards os

does anterior margin; narrowly elliptical with

greatest breadih medial aud over 1/3 length

(in males). Internally: lamellae rather nurrow;

line of conerescence marginal: inher margin

regular; marginal pore canals short and

numerous: selvaze very prominent in RY but

absent in LV; LV with series of shallow yen»

tral indentations to match RV denticulation;

normal pore canals scattered, simple, open;

centval muscle scars of usual cypridid pattern,

comprising 4 adductors and 2 mandibulars;

hinge consisting of RV ridge and LV groove.

Carapace sex dimorphism: females larger and

slightly broader than males.

Antennule 7-segmented; segmental length

ratios 64:17;22:13:11/9:9; terminal segment

over twice as long as wide; “natatory” setae

mare than twice as long as 5 distal segments

combined, Antennal endopod 3-segniented,

length ratios of segments 22:18;1,5; flagellum

teaching almost to middle of first endopod seg-

ment) “natatory” setae distal on this segment,

reaching fo tips of terminal claws, Mandible

eoxa normal. epipod with abour 6 Strahlen,

endopod « and @ bristles both slender and

pilose, y bristle thick and tapermg, adorned

oeur its end with spiky hairs, Maxillule epipod

with 3 downwards directed and 20 other

Steahlen; second palp segment cylindrical and

narrow: third lobe with 2 toothed Zahnborsten.

Maxilla (P 1) epipod with 6 Strahlen; female

palps similar with 3 terminal bristles, 2 sub-

equal, third about twice as long; male palps

dissimilar and modified as ¢lasping organs.

Walking leg (P IT) endopod 4-segmented; seg-

mental length ratiog 14:7:8:3: terminal claw

about half ugain as long as last 3 segments

combined, Cleaning limb (P TI) reflexed,

sender, normal, Chitin support with simple

distal points branched proximally, dorsal

branch short and sharply curved, ventral

bratich less curved and relatively long. Furea

with 2 claws and 2 bristles; length ratios for

fircal shaft:anterior claw:posterior claw 35:

20:12: length;width of shaft 15:1: bristles sub-

equal, posterior One separated by detinite gap

from posterior claw, Zenkers Organ (males)

with 30-31 whorls. Hemipenis subtriangular

With prominent antenor process and distinctly

downlutned fap. Cups of nauplius eye fused,

Dimensions: Halotype. adult male—L = 1.59

mm; MH = 1.13 mm; B = 0.63 mm. Panitype,

adult female—l = 1.90 mm; H = 1,43 mm:

B= 0.85 mm,

Discussion; Oyprinoins ws one of the more dis

finclive continental ostracode genera. and is

easily placed on carapace characters alone by

the RV dorsal hump and ventral marginal den.

AUSTRALIAN SALT LAKE OSTRACODA 183

Figs 35-50. Figs 35-37; Cytheroma sudaustralis n. sp., holotype, male. 35: hemipenis; 36: posterior

of body; 37: labrum, Figs 38-42: Cytheroma sudaustralis n. sp., paratype, AM P26653,

female. 38: posterior of body; 39: distal antennule; 40: P I; 41: distal P Il; 42: distal

P Ill. Figs 43-50: ? Microcytherura difficilis n. sp., holotype, male. 43: labrum; 44: distal

mandible covale; 45: antenna; 46: antennule; 47: maxillule palp and lobes (segments

only); 48: distal P T; 49: distal P Ill; 50; P TI. All magnifications x 600.

184 K, G, McKENZIF

ticulations. This species is more flexuous in

dorsal view than other known species, includ-

ing the two species previously described from

Western Australia—C. dahli Sars and C,

ward? was found in a collection made in

December 1976 by W. D, Williams on Kan-

garoo Island, S.A., so the species has a wide

distribution jn southern Australian salt lakes.

Derivation of name; For D. H. D. Edward,

who has made several excellent large collec-

tions of Western Australian entomostracans.

Subfamily; DIACYPIDINAE McKenzie

Diagnosis; A subfamily of cypridid Ostracoda

characterised by small-medium sub-nangular

or subrectangular smooth or reticulate cara-

paces and either lacking epipods on the Pl

altogether or having epipads with only 2

Strahlen. Confined to Australia,

Although first noted as distinctive by

McKenzie (1977b) the whove constitutes its

formal designation,

Discussion; The endemic Australian genus

Diacypris has been regularly referred to the

Eucypridinae Bronstein, 1947 (Danielopol and

McKenzie 1977). Bur unlike the eacypridine

genera, which are relatively large and typically

mytiliform in lateral view, Diacypris js smaller

and more regularly subtriangular in lateral

view; also, whereas all eucypridines have well

developed epipods with 6 Strahlen on the P 1,

the diacypridine venera ether lack an epipod

altogether, or have one with 2 Strahlen,

McKenzie (1971) suggested that (he presence

or absence of a P I epipod alone is insufficient

to separate genera which otherwise are Very

similar, In this instance, however, the eharac-

jer is only one of several by means of which

cucypridines and diacypridines cin be ensily

distinguished, as indicated above and as will

appear from the descriptions below, Originally

the group was proposed as a new tribe, bul its

status is now raised to subfamily fullowing the

rationale of Hartmann & Puri (1974) in their

recent general classification of Ostracoda,

MeKenzie (19776) noted that dincypridines

occupy in Australia the niches filled m South

Africa by cypridopsines. This is un instance

of habitat convergence, since taxonomically

the groups are Very distinct,

Genus: DIACYPRIS Herhst, 1961

Diaeypris dietzi (Herbst, 1958)

Localities: Several in S.A. (see Appendix IT).

This ts the most common Diacypris in the col-

lection.

Diacypris fodiens (Herbst, 1958)

Localities: Several loculities m S.A. (see

Appendix I).

Diueypris whitei (Herbst, 1958)

Localities; Several localities in SA, (see

Appendix 11),

Diacypris paracompactsa sp. nov

FIGS 11, 12, 31, 58-62

Malotype: AM P26669,, adult mule,

Pararvpes: AM P26670-26672, 3° adult

females, | adult mule.

Type locality: Very large shallow lake 15 kra

N of Kingston, S.A,

Marerial: A topotypic population and indivi-

duals from a small salt lake abonl 16 km N of

Meningie and two samples from the cut-off

portion near “Cantara’, The Coorong.

Description: Shell whitish; small-medium sized;

regularly subtriangular in lateral view; LV

jarger than RV, and overlapping it dorsally by

a low elongate ridge; micropunctate; dorsum

strongly convex, more so in LV, anterior

broadly founded; posterior more narrowly

rounded, trending posteroventrally; yenter

inflexed medially; greatest height medial, about

2/3 length. In dorsal view subelliplical, nar-

rowing anteriorly, more rounded posteriorly;

greatest breadth medial and just under hale

length, Internally; lamellae broad; line of con-

crescence submarginal; inner margin regular}

marginal pore canals mumcrous short ane

straight anteriorly and posteriorly, longer ven-

Figs 51-62, Fig, 51) 9 Microeythertra difficilis sp. nov. holatype. male, hemipenis. x 600, Figs 52—

57; Cyprinotes edward! sp. noyv., holotype, male, 52: antennule (segments only), x 150,

§3: mivallule palp and lobes (segments only) with Zahnborsten, » 150; 54; hemipenes,

x 624) 55; PW. x 150; 56° P I & £50; 57: PL & 150. Fig. 58, Diaeypris pareeemnpoela

gp. uv, paratype, AM P2667), female, maxillile palp and lobes (segments anly) with

Zuhnbarsien, x 600; Figs 59, 60, Piacvpris paracempacta sp, noV,, holotype, male. 59:

Yenkers Organ, « 600, 60+ furea. » #00 Fie. 61, Diaevpriy paracempacta sp. nov, para-

ire, AM P26670, femule. P I (without setation), noaie absence of epipod, x 600. Fir. 62,

Digevpris paracompdeta sp, nev., paratype, AM P26672, ovale, hemipenis, x 600.

185

AUSTRALIAN SALT LAKE OSTRACODA

AUSTRALIAN SAL'!

irally; normal pare canals scattered, simple,

open; muscle sear Weld posteramedial, com-

prising rosette of 4 adductors plus 2 mandi-

bulars: hinge consishng al RV ridge and LV

groove. Shell sex dimorphism weak, females

usually larger and with greater size range than

males.

Antennule 7-segmented: segmental length

ratios 70;20:20¢18;15°8;8: “natatory” setae

about four limes as long as 5 distal segments

combined, Antennal endopod 3-segmented;

length ratios of segments 23;14:4) “natatory”

setae extending beyond lerminal claws and

originating mediodistally on tirst endopod seg-

ment} flagellum reaching distal end of this

segment. Mandible coxa normal; epipod with

about 6 Strahlen; endopod normal, g and #

ventrwl bristles slender and pilose, y bristle

thick and tapering, about twice as long as

terminal segment. Maxillole epipod with about

20 Strahlen; palp cylindrical, narrow; length

ratio of palp segments 20/9; third lobe with 2

weakly toothed Zahnborsten; 2 shart bristles

proximally on first lobe, Maxilla (PT) epipod

absent; endopod mm female with 3 terminal

bristles, one short, second sbout twice as long

and third very lang; in males, endapods modi-

fied as asymmetnc clasping palps, right

hroader and less Mexaous than left. Walking

ley (P IL) endopod S-segmented (penultimate

segment undivided}; segmental length ratios

16:18:23; lenninal claw about as long as endo-

pod segments combined. Cleaning limb (P IIL)

reflexed, normal. Chitin supports with simple

point distally; branched proximally, with dorsal

branch about 2/3 length of ventral branch.

Fureal shaft gently curved, with normal com-

plement of claws and bristles; shaft:anterior

cliwsposteriar claw length rahos 40:30:13;

shaft lungthewidth abaut 20:1; bristles sub-

equally long, posterior bristle slightly displaced

from postenar claw. In males, Zenkers Organ

has 12-14 whorls, Hemipents with relatively

slrameht weakly bilobate anterior process; basal

process well chitinised and strongly curved.

Rake-like organs euch with & teeth, one bifid

Cups of nauplius eye fused,

’ LAKE OSTRACODA

187

Dimensions; Holotype, adult male—L = 0,55

mm: H = 040mm; B = 0,25 mm- Paratype,

adult female—L = 0,58 mm; H = 6.41 mm;

B= 6.28 mm.

Discussion: The posteromedial muscle sear

field and the relatively shortened antennale

segments are further characters which separate

diavypridines from ecucypridines, Male charac-

ters, such as the number of Whorls in the

Zenkers Organ and the hemipenis morphology.

are also distinct and unlike such features in

eucypridines,

The new speeies is very clase to B. coarn-

pacia (Herbst, 1958) but in that species there

is no dorsal overlap by the LV of the RV,

such as characterises paracomipucta. This fea-

ture also separates D, paracampacta from the

following species,

Derivation ef name: From the Latin para =

similar, and the species name compacta,

Diacypris oceldentalis sp. noy.

FIGS 7, 13, 14, 20

Holotype: AM P26673, adult male,

Parntypes. AM P26674, 2 adult females, 1

adult male,

Type locality; Lake Dumbleyung, W.A,

Material: Topotypic material ayd populations

from Lake Chidpup, Lake Stubbs, and New-

digate, a shallow sall water lake near Lake

Grace, all iv WAL

Deseription, Shell greenish in life; small-

medium sized; regularly subirmngular in

lateral view) almose equivalved: smooth: dor-

sum strongly =oconvex; onterior broadly

rounded; postenoer more narrowly rounded,

trending, pasteroventrally; venter inflexed

mediully; greatest height medial and over 2/3

length. In dorsal view subelliptical; narrowing

anteriorly and rounded posteriorly; greatest

breadth medial and about half length. Inter-

ually: similar to D. paracompacta. Sex dimer

phism weak, fermales usually larger than males.

The soft parts are closely similar to those of

D. paracumpacta except for these differences:

Figs 69077, Figs 63-65, Relievpris herbsti n, gen. 1, sp, holotype, male. 63: antenna endopod tseyvments

only); 64; PL right palp; @S) P 1, left palps Figs 66-69: Resievpris herbsti n. gen. n.

sp. paratype, AM P26678, female. 66: mundible endopod (segments only) with «, #

and > bristles; 67: P i 68: PIITL 69: masxillgle palp and thied Jobe with Zabnborsten.

Figs 70, 7h! Retievpris mn gen, n, $f. holotype, male. 7D; chitin support; 71> hemipenis.

Figs 72-77. Retieypris dedeckkeré nm. gen. nm, sp. holotype, male, 72: detail antennal

sensory seta; 73> disind furca; 745 right Pole 78: antennule (segments only}: 74: hermi-

nenis; 77> distal P th, All magnifications « 600,

188 K. G. McKENZIE

The length ratios fureal shaft: anterior claw:

posterior claw in D. occidentalis are 44229:15,

i.e. the shalt is slightly longer than in 2, pare

campacta. Further, the basal process of the

hemipenis in D, oceldenralis is thicker than In

DP, paravompacta, and ot similar thickness

throughout its Jength, not tapering as in D,

paracompacta; also, the anterior process does

not extend as far beyond the basal process as

in the South Australian species. The Zenkers

Organ has LI-]2 whorls,

Dimensions; Holotype, adult male—L = 0.56

mm; H = 0.38 mm; B ~ 0.25 mm, Paratype,

B= 0.28 mm.

Diseusyion: D. oceldentalis, like DB. compacta

(Herbst, 1958) does not have the same definite

LV overlap which chaructenses D. parucon-

paca. It isa distinctly smaller species than P,

compacta which has 4 length of about 0.71

mm and 14 whorls on the Zenkers Organ,

Nevertheless, the three species mist be con-

sidered a closely allicd group since their hemi-

penes are so alike.

Derivation of names From the Latin, acciden-

jalis = Western, a reference to the species’

Western Australian provenance,

? Diacypris sp,

Localities; Two localities in WA, (sce Appen-

dix LL) but the taxon ts known to occur also

in South Australia (De Deckker pers, comm.)-

Discussion: The shell of this species is charac-

terised by « pronounced overlapping hump in

the LV; und by the presence of several sirong

spines on the carapace, one or two anteriorly

and one posteroventrally on each valve. It is

unlike any previously described Diacypris tn

shell characters, and there were no soft parts

in the specimens encountered in thrs collection

De Deckker (pers. comm,) has indicated that

the soft anatomy 1 Uke Divevpris, OF the

three specimens available, the largest measured

0,70 mm.

Rerleypris gen. nov,

Type species: Retieypris herbsti sp. nov,

Diaynosix: Diacypridine genus characterised

by small-medium size; fenculute carapace;

maxilla (PL) epipod with 2 Strahlen; reet-

anvular hemipenis with downturned flap on

anterior provess; relatively smooth Zahn-

borsten on third tobe of maxtllule, Otherwise,

like Olaevprix in its soft anatomy.

Diseasyion: It is apparent that Reticypris,

especially im ils reticulate cayapace, is very dif-

ferent from Piaeypris. However, there are

some points of strong resemblance even in the

¢arapace, notably the posteromedial muscle

sear ficld, The ditferences are probably enough

to justify a new tribal category for Reticypris.

But with only one genus Known with certainty

for cach tribe such a move seems premalure,

although consistent with modern taxonomic

practice in which even subfamilies have been

named for single ostracode genera,

Derivation ef nante; Prom the Latin, rete = a

net and the generic suffix cypris; for (he rete

culate carapace, The genus is feminine,

Reticypris herbsti sp_ oov-

FIGS 15, 17, 35, 63-71

Holotype: AM P26676, adult male.

Paratypes! AM P26677-~P26679, 3

females.

Type locality: Very large shallow lake 15 km

N of Kingston, S.A.

Description: Shell whitish-brownish, smeall-

medium sized} subquadrate in lafecal view; 1n-

equivalved, LV larger and overlapping dor-

sally; reticulate and with weak ventral ridge

which is more noticeable in RV; dorsum gently

convex, inclined towards rear; anterior broadly

rounded: infiexed anterodorsally in RV where

LV overlaps it; posterior more narrowly

rounded; venter inflexed medially; greatest

height anteromedial (LV) and about 2/3

leneth, In dorsal view subelliptical; narrowing

unteriorly, more rounded posteriorly; greatest

breadth medial aod ahout half length. Inter-

nally! lamellae broad; line of concrescence

submarginal; inner margin regular; weak

selvage present in LV; marginal pore canals

numerous and straight; normal pore canals

scattered, simple, open; muscle scar field pos-

teromedial, comprising rosette of 4 adductors

plus 2 mandibulars; hinge consisting of narrow

RV ridge with small triangular anterior pro-

jection (unolislip clement) and accommodation

groove in LY. Shell sex dimorphism not

marked, females usually larger than males,

Antennule 7-segmented; segmental length

ratios 93;25;23:22:13:15.12; “patatory” setac

about 4 times as long as S distal segments

eombined. Antennal endepod 3-segmented;

segmental length ratios 22:13:15; flagellum

extending beyond distal end of first endopod

segment; “natatory” setae extending well be-

yond tips of terminal antennal claws and on

rinating medjodisially on first endopod seg-

ment, Mandible coxa normal; epipod with 6

adult

AUSTRALIAN SALT LAKE OSTRACODA 184

Strahlen plus basal seta. Maxillule normal;

epipod with about 20 Strahlen; length ratio of

palp segments 5:2; Zahnhorsten of third lobe

relatively smooth, Maxilla (P 1) normal, epi-

pod smal] bur distinet, bearing 2 Strahlen; male

palps asymmetric as in Diacypris, Walking leg

(P IC) with the penultimate segment undivided;

terminal claw powerful, curved ard about

twice as long as penultimate segment. Clean-

ing limb (P 111) normal; terminal segment

small but distinct, Furcal shaft evenly curved,

lengilt ratios of shaft:anlerior claw: posterior

claw 45:21:12; bristles ahout equal, posterior

one separated from posterior claw by small

pup. Chitin support with bluntly pointed distal

tip and forked proximally, ventral branch

almost twice as long as dorsal branch, To

tales, Zenkers Organ has 0-11 whorls; bemi-

penis is rectangular, anterior process with a

downturned flap. Cups. of nauplius eye fused,

Posterior of body without any prominent lobe,

Dimensions: Holotype, aduli: male—L = 0.54

mm; H = 0,38 mm; B = 0.25 mm, Paratype,

adult female—L — 0.58 mm: H = 0.40 mm;

B = 0.28 mm.

Derivation of name; For H. V, Herbst, who

deseribed Diaeypris.

Reticypris dedeckkeri sp, nov

FIGS 18, 19, 72-77

Holotype: AM P26680, adult male.

Paratypes: AM P26681-26682, 3

females, | adult mate.

Type locality: Small pond south of Yorketown,

S.A.

Description; Shell whitish-brownish; medium

sized; subreniform in fateral view: anequi-

valved, but not as markedly so as R, herhsti}

reticulate, Without ventral ridge; dorsum venily

convex but not so inclined towards rear as in

R, hevbsti; anterior and posterior about equally

broadly rounded in 1.V, anterior more broadly

rounded in RV; venter inflexed medially;

greatest height unteromedial and ubout 3/5

length, In dorsal view) with subparallel flanks:

more narrowed vanteriorly than posteriorly,

greatest breadth medial in males, slightly pos-

teromedial in females and about half length.

Internally: similar to R, herbyti. Shell sex di-

morphism not marked, females usually larger

and slightly broader than males.

adult

The soft part morphology is very similar to

that of R, herhyti, except that the length ratios

of furcal shaft:anterior claw:posterior claw are

50:23:12, ic, the shaft is slightly longer in

R. dedeckker|, Ta males, the Zenkers Organ

has 10 whorls in &, dedeckkeri and the hemi-

penis differences can be cheeked on the illus-

trations (figs 71, 76).

Dimensions: Holotype, adult male—L. =~ 0,68

mm; H = 0.40 mm; B — 0.3) mm, Paratype,

adult female—L = 0.68 mm; H = 0.44 mm}

B- 0,34 mm,

Discussion; The two species of Reticypris

deseribed above can be readily distinguished

on shell characters alone. Of the two, R.

dedeekkeri is much the larger, has a subreni-

form, rather than subquadrate, shape in lateral

view and no ventral ridge and ditfers alsa in

dorsal view,

At present R, dederkkeri is known only

fram the type locality,

Derivation. af name: Por P. De Deckker, who

has recently described two new Australian

astracode genera,

Other species

Several other species are present in the

material (Appendix 11), But they are listed in

open nomenclature and, except in the case of

? Diaeypris sp. whieh i very distinclive, no

further details on them are included, Usually,

there are fot enough specimens to base a

descriplion upon, In other cases, the available

specimens are either juvenile or occur us [rag-

ments only. Ohe specimen in sainple §.A. 40,

a Diacypris sp. with spinose yentral margins

and measuring 0.88 mm, was destroyed during

scanning electron micrography of the fauna.

Acknowledgments

Prol, W, BD, Williams collected the material

and kindly provided facilities at Adelaide dur-

ing the study. Dr C, Bartusek provided helpful

advice on the University of Adelaide's Siemens

scanning clectron microscope. Mrs A. Perry

and Mrs C. Kear typed the mratuseript. Mrs

SEM mnucrographs.

The research was supported in

A.R.G.C, Grant No, D76/ 151.27,

part by

190 kK. G, MeKENZIE

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NOTES ON THE BIRDS OF PEARSON, DOROTHEE AND GREENLY

ISLANDS, SOUTH AUSTRALIA

BY SHANE A. PARKER AND JOHN B. COX

Summary

Ornithological results of an expedition to Pearson, Dorothee and Greenly Islands off the west coast

of Eyre Peninsula in November 1976 include field observations, details of specimens collected, and,

for a few species, remarks on taxonomy, distribution, and food. Previous records are summarized.

New records are: White-faced Storm-Petrel (Pearson), Great Cormorant, White-faced Heron and

Turnstone (Dorothee and Greenley), Spur-winged Plover and Barn Owl (Dorothee) and Fairy Tern

and Little Grassbird (Greenly). On Big Veteran, a rock between Pearson and Dorothee from which

no birds have previously been reported, we noted six species: Great Cormorant, Sooty

Oystercatcher, Turnstone, Silver Gull, Pacific Gull and Rock Parrot. Also of special interest are

breeding colonies of Short-tailed Shearwater on Dorothee and Greenly, breeding colonies of White-

faced Storm-Petrel on Dorothee, a probable breeding colony of the Fairy Tern on Seal Rock off

Greenly, and breeding of the Welcome Swallow on Dorothee.

NOTES ON THE BIRDS OF PEARSON, DOROTHEE AND GREENLY

ISLANDS, SOUTH AUSTRALIA

by SHANE A. PARKER* and JOHN B. Cox?

Summary

PARKER, S. A, & Cox, J. B. (1978) Notes on the birds of Pearson, Dorothee and Greenly

Islands, South Australia. Trans, R, Soe. 8. Aust. 102(7), 191-202, 30 November, 1978.

Ornithological results of an expedition to Pearson, Dorothee and Greenly Islands off

ihe west coast of Eyre Peninsula in November 1976 include field observations, details of

specimens collected, and, for a few species, remarks on taxonomy, distribution, and food,

Previous records are summarized. New records are: White-faced Storm-Petrel (Pearson),

Great Cormorant, White-faced Heron and Turnstone (Dorothce and Greenly), Spur-winged

Plover and Barn Owl (Dorothee) and Fairy Tern and Little Grassbird (Greenly), On Big

Veteran, u rock between Pearson and Dorothee from which no birds have previously been

reported, we noted six species: Great Cormorant, Sooty Oystercatcher, Turnstone, Silver

Gull, Pacific Gull and Rock Parrot. Also of special interest are breeding colonies of Short-

tniled Shearwater on Dorothee and Greenly, breeding colonies of White-faced Storm-Petrel

on Dorothee, a probable breeding colony of the Fairy Tern on Seal Rock off Greenly, and

breeding of the Welcome Swallow on Dorothee,

Introduction

In November 1976 a biological survey of

Pearson I, and Dorothee TI,

Group) and Greenly & was undertaken by

A. C, Robinson, T. J. Fatchen, A. Spiers and

J, B, Cox (S.A. National Parks and Wildlife

Service) and W, Zeidler and S$. A. Parker

(S.A. Museum). Here we present the orni-

thological results, including some sightings

made in Coffin Bay on the opposite mainland,

and on passage between Coffin Bay and the

islands,

Previous observations (summarized here)

are available from Pearson for 1914, 1920,

1960, 1969, 1973 and 1974, from Dorothee

for 1969, and from Greenly for 1947. Cleland

(1923) gave details of birds noted on Pearson

in Junuary 1923, and Paton (1971) of birds

on Pearson and Dorothee in January 1969,

Both authors referred to observations made on

Pearson by E. R. Waite in September 1914

and F, Wood Jones in November 1920. In

additlon, Paton included observations made

by I, M, Thomas and 8. J. Edmonds on

Pearson in January 1960, Hornsby (1978) pre-

(Investigator

sented observations made on Pearson in Feb-

ruary 1973 and February 1974, The previous

records from Greenly are those of Finlayson

(1948) for November 1947 and Mitchell &

Behrndt (1949) for December 1947.

List of species

Eudyptula minor (Forster), Little Penguin

Pearson I. Noted on all previous visits, on

all sections, burrows being found yp to more

than 150 m as. (Paton 1971, Hornsby

1978). We found many burrows (Fig. |) in

the friable soil in crevices amony boulders, and

in steep slopes, usually under low shrubs, e.g.

Rhagodia crassifolia, Olearla ramulosa, These

contained eggs, chicks at various stages, and

moulting adults,

Dorothce I. Previously recorded by Paton

(1971), We found fewer than on Peurson L,

and only on the northern half (Fig. 2), mainly

in crevices among rocks under dense low

shrubs: one bird was incubating an egg.

Greenly I. Reported by Finlayson (1948)

and Mitchell & Behrndt (1949) on the slopes

of the south section up to ¢¢ 123 m, The latter

* South Australian Museum, North Tee: Adelaide. S. Aust. 5000,

+ 48 Carter St. Thorngate, S. Aust, 5082,

192 SHANE A. PARKER & JOHN B. COX

NORTH

SECTION

781 HILL

MIDDLE SECTION

&/ Landing

Beach

TU ine Penge

Yorirrp satan Seip

ESSE ster) snus haarnenes

Fig. 2. Dorothee Island.

authors noted that in December 1947 breeding

appeared to be over. We found the species

halfway along the sloping north face of the

south section (Fig. 3), in burrows in soil-filled

rock crevices usually overhung by tussocks of

Poa poaeiformix. All birds in the burrows Were

in heavy moult.

The species was also noted breeding on

islands in Coffin Bay, 1.xii.1976: one dead

Wanda Point

NORTH SECTION

Fig. 3. Greenly Island (key as for fig. 2).

chick on the main island of The Brothers; two

adults, one on eggs, on Garden L., with at least

twelve burrows in all, in soil beneath a 3m

limestone overhang.

Diomedea melanophrys Temminck. Black-

browed Albatross

Greenly I. One adult flying west. close in»

shore, 29.xi.1976.

Diomedea chlororhynchos Gmelin. Yellow-

nosed Albatross

Pearson I,: two swimming round fishing

boats in bay east of middle section, ii,1974,

and others between Pearson I. and the main-

land (Hornsby 1978). Greenly I.: one flying

west, inshore, 29,xi.1976; single birds 4 km

and 10 km north of Greenly I. 1-xii.1976. Near

mainland: single birds 15 km south-southwest

and 3 km southwest of Point Sir Isaac, Coffin

Bay Peninsula, 1-xii.1976,

Diomedea cauta Gould. Shy Albatross

One following boat continuously between

Dorothee I. and Greenly I., 27.x1.1976; two

inshore at Greenly I, 29-30.xi.1976; one 3 km

off Point Sir Isaac, 1.xii.1976 (all immatures).

Puffinus carneipes Gould, Fleshy-footed

Shearwater

First seen (one bird) 2 km northwest of

Point Sir Isaac, thence continuously (singly or

in small groups) to 40 km from Pearson I,

22.x1.1976. Common from Dorothee I. to

Greenly f., 27.xi,1976, in parties of up to 40,

often mingling with flocks of Short-tailed

Shearwater P. fenuirostrix, Many seen from

Greenly [. to Point Sir Isaac, 1.xi1.1976. At

sea, P. carneipes was more frequently encoun-

tered than P. tenuirostriy; individuals of the

former were scattered over a wider area and

tended not to form large flocks, whereas indi-

viduals of the latter were usually seen in very

HIRDS OF PEARSON. GOROTHEE AND GREENLY ISLANDS 193

large locks, 2. fennirostris was less abundanr

than P. carheipes over inshore waters of the

mainland, but about the islands the reverse ‘was

usually the case

McKeun (1963) presented evidence that

some individuals from the colony an Lord

Howe [. foraged off the coasts of New South

Wales and southern Queensland during the

breeding season, Such long-distance foraging

raises the possibility that the large numbers

seen in South Australian waters during the

breeding season are from Western Australian

colonies, rather than from as yet undiscovered

colonies in South Australia (see also Serventy

et al. 1971, Cox 1976),

Puffinias tenwirostris (Temminck), Shoart-taled

Shearwater

Pearson I, We néted five single birds within

10 km of the island an 22.41.1976, and trom

then till 25.%.1976 saw large numbers otfshore

cach day in the late afternoon or evening,

Serventy ew (1971) fisted Pearson I. as a

breeding station, bul although we searched the

island by day und by night, we found no signs

of 4 breeding colony.

Dorothee t. No previous records, We dis-

covered a breeding colony of ca 800 pairs on

the southern half of the island (Fig. 2), in an

area of granitic shale with pockets of softer

soil. The hurrews tended to be in the soil, and

many had their entrances overhung by the suic-

culent Disphyma clavellatum. Each burrow

examined contained a bird sitting on an egg.

This colony overlapped a colony of the White-

faced Storm-petrel, whose burrows tended,

however, lo be among Arriplex paludasa in the

shaly ground.

Greenly J, Finlayson (1948) found mummi-

fied remains beneath what appeared to be the

feeding tree af a White-bellicd Sea-Easle on

the ridge of the South Section, Mitchell &

Berndt (1949) obseryed several birds Sying

ahout the boat us i approached Tapley Bay,

und on the eastem end of the south section

found a series of burrows thar had apparently

not been used for several seasons, We located

a breeding colony on the steep southern slope

of the south section (Fig. 3)> if accupied the

only patch of sand and soft travertine noted by

us On the island. Most of the ca 200 burrows

had thetr entrances curtained by shruhs of

Enelylaena tamentasa, and most of those exa-

mined contained birds sitting on eees,

Miny individuals were seen inshore at

Greenly [., mainly in morning and tate after-

moon, 28-30-x1.1976, The species Was common

between Greenly [. and 20 km northeast on

|.si1976, becoming progressively scurcer to-

wards the mainlund. On 27.41,1976 we ob-

served large flocks of up to 150 individuals

continuously between Dorothee J. and Greenly

L, well away from land

Specimens: B3Nd63, Greenly 1, 30.47.1976, adull

male, tesies slighily enlitged (regressing)) skull

Mwily preumatized: colours (2 brs after death):

fees pile blac grey on inner faces. blackish outer.

outlet foe blackish, (wo inner loes pale lilac grey.

webs cream With greyish and blackish sireaks

(hevvier on undersurface): iris very dark brown;

upper mandible: angus black, rest blackish grey.

lower mandible: ramijcorn light grey, rest dark

Srey; eyverim blackish; slomuch contents: beaks of

small cephilopods. Bird taken 1030 hires while in

cubating ege (B30487, dead fresh) in large bare

sundy burrow about | m long, entrance curtained

by bush of Enehylaena fomeniosas tree braod-

Pulch On ahdomen,

H30464. Dorothee f. 26.x1.1976, dult female,

oocytes slighlly enlarged (? regressing). skull

poeumatization not recorded; colours (3S mins

afier deuth): legs lilac grey on inner faces, black~

ish grey on outer, outer toe blackish erey, two

inner toes lilae grey, webs greyish cream uohove,

cream with blackish streaks below: |ris very dark

brown, upper mandible; latericorn brownish prey,

rest blackish; Jawer mandible; camicorn medium

grey, unguis blackish, rest blackish distally,

lightening to grey at base; mouth: greyish white

linged with pink, tongue creamy pink; eyerim

black: Stomach conlents: black beoks of small

cephalopods. Bird token late affernoon incubating

eee, (R30486. dead fresh), in large bare burrow

about | m long, roof 75 mm thick, under shrubs

of Disphyma clayellatum.,

Pelagodroma marina (Latham). White-farced

Storm-Petrel

Pearson [, No previous records, Affer dark

om 24 and 25,x1.1976 we noted one or two

flying above our camp on the middle section:

one of these wis collected. We alsa found a

few feathers on the northern slope of South

Hill on the south section, We failed to find any

burrows, however. despite spotlighting and

daytime searches; possibly here, and on

Greenly |, the species is discouraged from

breeding by the presence of the Southern Bush-

rat Raituy fuseipes.

Dorothee [ Paton (1971) found the wings

of at least ten of these petrels in Front of small

burrows. We locared three breeding colonies

(Fig. 2), mainly among drriplex paludosa,

Threlkeldia diffusa and Rheagedia cravsifolia an

high shaly slopes, the burrow-entrances diffi-

14 SHANE A. PARKER & JOHN B, COX

cult to find among the dense shrubs. The most

northerly colony consisted of ca 70 pairs, the

middle colony of ca 200 pairs and the Jarge

colony around the southers hill of 1 L00-1200

pairs. The last overlapped a colony of Short-

tailed Shearwaters, who tended to burrow in

patches of solter graund amidst the shale,

Many wings and feet of the storm-petrels were

littered ubout these colonies. The Southern

Bushrat does not occur on Derothee f., and

the other noted predator of the White-laced

Storm-Petrel, the Black Tiger Snake Nolechis

sentatis (Wood Jones 1937), was also

appurently absent. We suspect that the pre-

dators were Pacific Gulls (see Littler 1910)

and = pair of Barn Owls [sce heluw).

We noted six solitary birds about midway

hetween Dorothee and Greenly on 27.41,1976,

und three others feeding tovether over calm

water in Coffin Bay ca | km east of Point

Longiose on 1,xi1.1976,

Specimens: B30465, Pearson 1, (middle section).

24.x1,1976, adult female, oocytes slightly enlarged

(? regressing); colours (10 mins after death, taken

in urtificial light); legs black, toes bhick except

for light blue-grey borders where they met webs,

webs cream with ureyish-black stripe in centre of

each) iris umber; bill black; mouth: palate dark

grey, pharyax pitkish white; eyerim black;

stomach contents (preserved) planktonic larvue of

crabs. Bird shot 2230 hrs (after dark), possibly

uttracted by campfire,

A20466, Dorothee L. 26.41.1976, adult female.

oocytes very sfighily enlarged (? regressing), ovi-

duct dilated and convoluted; most of skull

apparently one-layered bot hard; colours (before

death}: legs and toes black, centres of webs

creant; iris very dark brown; mouth flesh-grey:

eyerim) black: moderate subcutaneous fat, Bird

caught 1120 hrs incubating egg (B30488, incuba-

tion 0.2) at end of burrow; colony of ea 70 hur-

rows on eustfycing slope Of granitic rocks and

ahale, entrances difficult to find among low shrubs

of Threlkeldia diffusa, Atriplex palvdosa und

Rhageodia crassifolia.

B30467, Dorothee 1, 26.17.1976, adult mate,

lustes very slightly enkuged (? regressing); skull

fully pneumatized, colours (hefore death): was

R4046h: stomach contents one smal! stone; mwoder-

ale subcutaneous fat Bird cought 1145 hrs incu-

buting ege (R30489, Incubation 0.3) at end of

turrow, sume colony us BI0466.

Sula serrutor (G. R- Gray). Australasian

Gannet

Hornsby (1978) reported one seen regularly

off Pearson TL. m Bebruary 1°74. We noted two

al Pearson 1. on 23 and 26.x11976, eight be-

iwcen Gireenly 1, and Coffin Bay Peninsula on

}.x1i1.1976, and single birds off Point Longnose

and 2 km off Point Sir Isaac on 22.xi.1976.

Phalacrocorax carbo (Linnacus), Great (Black)

Cormorant

Noted in small numbers on Pearson 1, in

1923, 1960, 1969 and 1974. We observed up

to five together on Pearson 1,, and small num-

hers on Dorothee, Big Veteran and Greenly,

Phacton rubricavda Boddaert, Red-tailed

Tropic-bird

Clelund (1923) reeorded two oo the north

section of Pearsoj |. There ure only two other

records from the Eyre Peninsula region: a

female (SAM 62421) collected on Grantala

Farm, North Shields, north of Port Lincoln,

13.4,1919 (Cleland 1923), and a bird shot on

Flinders L, xii.1960 (Eckert 1970, Bedford

1972).

P. ruhricauda is a rarely reported visitor to

South Australia, records falling in the period

December-May, This period is its breeding

season in Western Australia (Serventy et al,

1971, Tarburton 1977), Eekert (1970) specu-

lated that it may have bred undetected on

islands off the South Australian coust.

Ardea novachollandiae Latham White-faced

Heron

Pearson [. Noted 1923, 1964, 1973 and

1974, We recorded one bird on the northern

Up of the north section, on rocks among

Cusuarina stvicta

Dorvthee 1, We saw two single birds at

opposite ends of the island, among boulders

hallway up the slopes,

Greenly I, One noted by us, among Casta-

tli steicta on the ridge of the south section,

Egretta sacra (Gmelin), Reef Heron

Recorded on Pearson 1,, 1920, 1923, 1973

and 1974. We observed one durk-phase indi-

vidual on the south section, perched on a

boulder halfway up the slope,

Cercopsis novachollandiae Latham, Cape

Barren Goose

Pearson Lo Noted on all previous visits. Tn

1976 we recorded two immatures and u dead

adult on the gorth section, in low open Mela-

lence lanceolata,

HIRDS OF PEARSON, DOROTHEBE AND GREENLY ISLANDS ys

Dorothee |, Previously recorded hy Paton

(1971), We noted a purty of nine adults on

the southern coast.

Greenly I, Recorded by Pinlayson (1948)

and Mitchell & Behrndt (1949),

Pandion huliaetus (Linnaeus). Osprey

Recorded only by Hornsby (1978), Whe tn

February 1974 saw one flying wlong the eastern

coastline of Pearson 1,

Haliacetus lencogaster (Gmelin), White-bellicd

Sea-Eagle

Pearson |. Cleland (1%23) noted at teasi one

on the north section, and found an old nest

possibly of this species near the summit of the

south section, Paton (1971) reported an un-

necupied nest on the south section, Hornsby

(1978) recorded two adults and a large im-

mature, mainly on the worth section, in 1973,

and in 1974 two nests on the north section,

one unoccupied but containing the skull af a

Southern Bush Rat, the other attended by two

adulis, We noted two adults, mainly over the

north section.

Dorothee |. Paton (1971) observed two

birds over the island, and found an unoceu-

pied nest on the peak on the southern part

Greenly T, Finlayson (1948) teported a

“Sea-cagle of Fish-Hawk .., seen at a distance

several times... could not be positively idep-

tifed". He photographed a nest containing

what he thought was a large fledgeling Osprey.

We consider the photograph (cover of 8. Aus.

Om, 18(8)) of insufficient quality for one to

be able fo say whether the bird is a young

Osprey or an adult or subadult White-bellied

Sea-Eagle, Finlayson also reported a feeding

tree of a sed-eugle on the high ridge of the

south section; beneath this were the remains

of « Short-tailed Shearwater, a Galgh, Tammar

Wallibies (Macropus ¢ugenti) and a Harra-

coula | Leionura atun)., He noted that the wal-

laby mortality on Greenly was considerable,

anid considered the White-bellied Sea-Eagle the

most likely predator,

Mitchell & Behrndt (1949), under “White-

hesded Osprey’, noted that a pair had taken

up “permanent residence” on the island, They

found two eformous nests near the surairnit of

the seuth section and another on the north

section, About the nest-sites, and beneath

several large Casuarina trees, were the remains

of numerous wallabies, The predator involved

was again almost certainly the White-bellied

Sea-Eagie. We noted two adults on Greenty,

usually over the high Cayvarina-clad ridge ef

the south section,

Falco cenchroldes Vipors & Horsfield.

Nankeen Kestrel

Pearson I. Reeorded 1923, 1969, 1973 und

1974, from ull three sections but no more than

two birds each time, We noted a pair with

fying young on North Mill (north section),

and located a second pair, possibly nesting, on

South Hill (south section), from an inacces-

sifle stick nest on the south face of which

came the sounds of cheeping, A single bird was

also seen hunting over the plain of Diyplryma

clavellatum and Atriplex paludosa on the

eastern side of the north section,

Dorothee |, Two noted by Paton (1971),

We ubserved two single birds at opposite ends

of the island,

Greenly {, Mitchell & Behmdt 11949)

teported a single bird preying oo the abundant

skink Egernia mu|tiscntata, We noted one hird

oVer the dense Melalevea lariceelate thickets

on the steep southern slope of the south sec-

Hon.

Haematopus fuliginosus Gould, Sooty Oyster-

catcher

Pearson [, Recorded on all previous visits

except 1920. We noted at least eight pairs on

the rocky flats and shorelines. One pair on the

middle section had a large flightless young one

that hid in low Adriplex; the parents were voci-

ferous, and one gaye the broken-wing display,

All adulls were in pairs save for the party of

seven thar New over the middle section carly

on 25,47, 1976.

Big Veteran, A pair seen from the boat.

Dorothee [. Paton (1971) recorded three

adults and a flightless young. We noted five lots

of three, three, three, five and one adults, but

saw fio signs of breeding,

Greenly 1. Finlayson (1948) recorded a pair

at the landing in Tapley Bay in Noveniber

1947. The following month, Mitchell &

Behrnde (1949) noted many in the same bay.

We saw a pair on the north section, but none

on the south section,

Vanellus novaehollandiae Stephens, Spur-

winged. Plover

Pearson I Cleland (1923) noted three in

Junuary 1923. Hornsby (1978) recorded three

in February (973 and two in February 1974.

196

We recorded two over the sea to the cast of

the middle section, and one over the sea off the

southern coast of the south section.

Dorothee l. We made two sightings, of two

and four birds,

Charadrius rubricalfis Gmelin, Hooded

Datterel

Recorded only by Hornsby (1978), who in

February 1973 saw two feeding aniong the

intertidal rocks of the isthmus between the

north and middle sections of Pearson |

Arenaria interpres (Linnacus). Turnstone

Fearson L. Paton (1971) ooted eight on the

north section. Hornsby (1978) recorded the

species in 1973 ad 1974, including a flock of

40 in 1974. We noted a flock of 19 on the

rocky eastern shore of the middle seetion.

Big Veteran, Four seen from the boat,

Dorothee [. We noted four on the southern

end,

Greenly I, We noted two in the channel

between the two sections,

Calidris ruficollis (Pallas). Red-necked Stint

C. alba (Pallas), Sanderling

Pearson |. in January 1960 Thomas and

Edmonds recorded individuals of either C, ri¢fl-

(1978) made similarly indeterminate sightings

in Febevary 1973 and February 1974. We

an ihe eastern side of the middle section.

Sterecorartus parasiticus (Linnueus). Arctic

Jaeger

This is the most frequent small skua in South

Australian waters, oecurring a5 a non-breeding,

mainly summer, visitor, We saw single birds

15 km northwest of Point Longnose on

22.41.1976. and midway beiween Dorothee

and Greenly on 27.x1-1976, The two pajrs of

small skuas noted by Finlayson (1948) on

Greenly in November 1947 may well have

been of this species.

Larus novachollandiae Stephens, Silver Cell

Pearson 1, Noted on all previotis visits except

1914.

Deorothec f, Recorded by Paton (1971),

Greenly 1, Recorded as not plentiful in,

November 1947 by Finlayson (1948), and in

the follawing month as visiting the island in

big flocks nd roosting on Seal Rock by

Mitchell & Behrndt (1949),

SHANE A, PARKER & JOHN B. COX

We noted the species on all (hree mlupds and

uo Bre Veteran, singly and in groups of up to

12. frequenting the consts

Larus pacilicus Latham, Pacific Gull

Pearson |. Noted on all previous visits. We

recorded ¢ight pairs of adults and five sub-

adulls, mainly inland and on the sandy beach

of the middle section. One pair kept flying

over a large flightless chick that skulked in low

shrubs aod crevices in a flat rocky area of the

middle section. Wood Jones found a nest-with

two eggs on 25,xi,1920 (Cleland 1923).

Dorothee 1, Two adulis recorded by Paton

(1971). We noted three pais (one with a

large fightless chick) and three subadults,

Big Veteran. We saw one pair from the

boat

Greenly 1, Recorded by Finlayson (1948)

and Mitchell & Behrndt (1949), The latter

authors reported the species as numerous, und

folind a nest on the north section contiining

two well-developed young, We recorded one

paiy of udulty and a subadult near the channel

between the two seeuons.

Specinens; BI04d68, Pearson [, (middle section),

72.x1.1976, subndult female, Gocytes not enlarged,

oviduet not convoluted: skull fully poeumutiwed,

colours (10 mins after death); legs and feet pale

Yellow faintly Unged yvreenish, claws black; ims

cream, heavily tinged dusky: bill waxy yellow,

tinged greenish, tips of mandibles orange-scarlel

with black along distal sections of tomia and bluok

smudges elsewhere in the scurle| field; mouth:

palate pale yellowish buff, tongue pale fleshy

Grange, rest light greenish yellow; eyerim ochra-

vcous yellow: stomach contents a few ehiton frag-

ments. Collected 1645 hrs among boulders on

coast, one of four birds, two adull4é and one other

subadult, Plumage adult except for wings ond tail.

830469, Pearson I, (middle section), 22,.1,1976,

adult female, four oocytes slightly enlarged (? re-

eressing). ovicuer convoluted; skull fully pneuma-

tized: colours (5 mins after death): legs und feet

(hull lemon. with pale grey in creases and on webs.

claws black; iris cream; bill dull waxy yellow

linged erecn, tips orange-scarlet with distal lomia

blicks mouth: pharynx orunge-pink, tongue

brange, rest dull yellow, siomach contents; three

chitons, Collected 1620 hrs, flying over sundy bay

bucked by Jurge smooth boulders.

B30470, Dorothee T., 26.43.1976, adult (skele-

lonized, nol sexed), skull fully pneumatized:

ewlours (10 mins after death): legs and feet yel-

low-grey, claws blick. iris white; bill rich yellow,

tips ted with distal fomia black; mouth; palate

yellow, gupe and tongue orunge: eyerim orange:

yellow, Collected 1935 hrs on rocky slope: with

vpother adult and (wo immatures, and attending

one large flightless juvenile.

BIRDS OF PEARSON. DOROTHEF AND GREENLY ISLANDS 197

A30471, Greenly 1, (north section), 28.%1,1976,

adull male, lesles somewhat enlarged (7 regress-

ing), skull fully pncumatized; colours (imme-

diately after death): legs and feet bright yellow,

chiws black; iis white; bill rich yellow, tips red,

Uisral Tomi black; mouth: palate yellow, gupe and

longue orange; eyerim orange, Cuflected 1850 hrs,

iyi ever rocks.

feod. The two stomachs examined con-

tained only the remains of chitons. Stirling

etal, (1970) reported many chiton shells in

regurgitured pellets at a nesi on the South

Neptunes. Other items of food fecorded for

South Australian populations include turbos

(molluses) and various sea-urchins, both

dropped from a height and smashed (Condor

1938, Collon 1960), the gastropods Subninella

undulera, Nitella torquata and Euninella

frunert (Cotton (960), rock crabs (Cleland

1923), parrot-lish pirated from fishing fines

(Mitchell & Behrodt 1949), placentas and

vomit of the Fur Seal Arctocephalus forstert

und seeds of Nifraria schoheri {Stirling et al.

1970) and immatures and adults of the White-

faced Storm-Petrel (Wood Tones 1937; see alsa

Littler 1910). (For comments on the dropping

behaviour of this gull, see Farr 1978.)

Taxonomy; Our specimens are referable to

the western subspecies L.p. georgii Vigars,

which breeds eastwards to Kangatow Island

and which diflers front the nominate subspecies

of Tasmania in having a blackish patch along

the distal tomia of both mandibles in the adult

(Van Tets in Frith 1977).

Sterna nereis (Gould), Fairy Tern

Pearson 1. Paton (1971) recorded two fish-

ing off the eastern bay of the north section, In

February 1974 Hornsby (1978) found two

colonies of abou! 30 birds cach on the lime-

stone plateau of the south section, nesting

amidst the low Arriplex. The nests contained

eggs und newly-hatched young. We noted up

to five birds fishing in the calmer waters of the

three bays west and east of the middle section,

Greenly I, We recorded ca 100 on Seal

Rock, Many were sitting, possibly on egps,

Individuals from this colony were scen to fly

westwards along the coust of the south section

16 fish near the chatinel, then return lo Seal

Rock.

Spectiens: B30472, Pearson T. (middle section),

24.xL1976. adult male in breeding dress, testes

much enlarged, skull fully poeumutized; colours

(5 mins after death); legs and feet orange yellow:

wis very dark brown; bill bright yellow, tip black-

ish, eXtreme lip whitish; mouth flesh grey; eyerim

bluck. Collected 0820 hrs over sea near beach;

with Unree others.

830473, Greenly |, (south section), 29.x11976,

udali male in breeding dress, tesies much enlarged,

skull fully pmeumatized: colours (shortly after

death): legs ond feet orange yellow, claws black;

ivis very dark brown; bill rich yellow, tip of upper

mandible blackish; mouth; pharynx pale purplish-

pink, palate creamy pink, inner bill and gupe dull

yellow; everim black; stomach emipty. Collected

0925 hrs, diving ulong rovky coast,

Sterna bergii Lichtenstein. Crested Tern

Pearson I, Recorded on all previous visits

except 1914, We noted a Hock of 210 sitting

on rocks near the landing on the nvddle sec-

tion, and one and four birds off the south and

middle sections respectively.

Dorothee 1, Paton (1971) recorded ca 100

resting on the rocks at the southern end, We

saw two single birds flying offshore.

Greenly [, Mitchell & Hehrndt (1949)

recorded several small fiocks about Tapley Bay.

We noted a flock of 127 on the north section,

just south of Wandra Point. behaving as

though about to hreed-—grouped mainly in

pairs and behaving aggressively,

Cacatua roseicapilla Yivillot, Galah

Pearson I, Hornsby (1978) recorded this

species twice in February 1973—a pair, and

later a lurge flock. flying from Pearson 1,

towards Dorothee,

Greenly |. Finlayson (1948) found the

remains af a Galah beneath the feeding tree

of a White-bellied Sea-Eaglie on the south sec-

tion.

Other oilshore islands on which this species

has been recorded (mainly since the 1930s)

are Kangaroo, Wardang, Troubridge. Althorpe,

South Neptunes, Reevesby and Flinders, On

Althorpe I, it has been reported nesting in the

cliffs, and may also do so om Kangaroo 1, and

Flinders 11

Neophema petrophila (Gould). Rock Parrat

Pearson J. Recorded on sll previous visits.

We noted af least 16 on the south section, five

on the middie section and seven on the north

section, Two specimens collected on the south

' Parker, S. A., Eckert. H. J. Ragless, G. B.. Cox, FB, & Rei, N, C. H. (in prep.}, An Annotated

Checklist of the Birds of South -Australia.

198 SHANE A. PARKER & JOHN B. COX

section, 23,xi1,1976 (see below), were judged

by B. Hutchins and F. Lewitzka (pers. comm, )

to be ten weeks old ie to hove edged three

weeks previously. The species was recorded in

all habitats, including bare flat granite rocks,

low Atriplex and the Casuarina woodland of

the north section, We noted the call as a high

double-whistle, repeated,

Big Veteran. We observed four from the

boat,

Dorothee 1. A few recorded by Paton

(1971), We counted 33-35 birds. including, a

flock of 20 moving restlessly through Arriplex

shrubs among boulders on a steep slope.

Greenly [, Mitchell & Behrendt (1949)

recorded several flocks arriving, and others

departing in a direet line to the mainland in

December 1947. None was recorded by Fin-

laysen (1948) the previous month, nor did we

encounter tt. Mitcbell & Behrndt suggested

that (hey migrated to the island to feed on pig-

face (Aizoaceac) seeds,

In South Australia the Rock Parrot breeds

on several islands off Eyre Peninsula cast Lo

the Sir Joseph Banks Group, and on an island

in Pondalowie Bay, southern Yorke Peninsula.

In the non-hreeding scason it disperses to the

opposite mainland, to other islands (ucluding

Kangaroo |.) and eastwards and southwards

alont the coast at Jeast us far as the Baudin

Rocks near Rohe!, It fs noteworthy that there

are no breeding records of this parrot from

Pearson, Dorothee or Greenly; this may he due

to the paucily of observations during the

breeding season (eggs late Auig.-carly Nov,),

ar ty the absence or wear-ahsence of suitable

nesting-sites on these ishynds (crumbling,

fissured limestone faces draped with suceu-

ents).

Specimens: B3U474, Pearson T. (south sectios),

23.41.1976, immature male about 10 Weeks old,

testes not enlarged, skull fully preumatized:

colours (4 mins efter death)» legs pale fnlly grey,

logs preyer. claws black; iris very dark Urown,

upper mandible und cere oiminiy dull prey. with

nostrils, proximal tomia and distal culmen onnge

bull, tower mandible Orange bull) mouth pate

Orange-vellow tinged preys eyerim dark grey: crop

contenils (preserved); seeds. Collected |100) hres

among lorge granite boulders above small bay:

with une other bed

B3047S, locality-skull data as B30474; colours

timmedintely after deatt)> legs wnd feet creamy

miey; is Very dack browns Upper mandible olive-

harn. toma vellow: lower mandible yellow! cere

greyish yellow; mouth pinkish yellow; eyenm

blackish: crop contents (preserved); seeds, Col-

lected 1105 brs among large grunite boulders on

coast: with ane other.

Food: The crap of 830474 contained chiefly

the seeds of Lepidiia foliosum, Correa reflexa

and a species of Atriplex; a minuie reddish

sted of an nizoaceous species (vither a Curpo-

hrotus sp. or Disphyina clayellatum) was also

present, in a small quantity. The crop of

630475 contamned only the seeds of a Rhayo

dia sp, (1. Williams i lit, Svii,1977)

Melopsittacus undulatus (Shaw), Budgerygah

Recorded only by Paton (1971), who saw

two On the north section of Pearson 1.

Chrysococcyx basalis (Horslielc), Horsfield’s

Bronze Cuckoo

Al least two seen by Cleland (1923) on

Pearson J,

Tyto alba (Scopoli), Barn Owl

Pearson 1, Under Owl, Cleland (1923)

wrote. “A farge bird seen once at night anid

pellets found near the northern summit, suygesc

the presence of un Owl.” Hornsby (1978)

reparied a Barn Owl io the upper part of Main

Creek, porth section, in February 1973 and

February 1974.

Dorothee T, On 26,x1,1976 we flushed two

Barn Owls from a crevice umong large boul-

ders near the top of the cleft running across

the waist of the island, In the crevice were

feathers of the White-faced Storm-Petrel

(qv),

In South Australia the Barn Owl is known

mainly from the eastern part of the State, with

records also from the Nullarbor Plain and

Eyre Peninsula. Apart from those mentioned

above, it has been recorded on the following

islunds, presumably mainly as a vagrant dues

ing ituptions: Kangaroo, Goose, Wardang.

Thistle, Wildegrave, Franklin (Parker 1977)

Apus pacifiess (Latham). Fork-tailed Swift

Paton (1971) recorded at Jeust 20 hawking

over the northern peak of Dorothee on

TL 1969,

Hirundo neoxena Gould. Welcome Swallow

Pearson [, Recorded on all visits except

1914 and 1920. We saw it frequently on all

sections, in wnes, twos, threes and fours, and

once in a flock of ee 30 above Casuarina stricta

woodland on (he sheltered northeastern slope

of 78| Hill on the north section

BIRDS OF PEARSON, DORUTHER AND GREENLY ISLANDS

Dorothee 1, Noted by Paton (1971) as

probably the most common species on Doro-

thee and Pearson next to the Silvereye Zoy-

terops lateralis. We saw a pair at the northern

tip and a single bird on the southern coust.

Greenly 1, Recorded by Finlayson (1948)

and Mitchell & Behradt (1949), We noted af

least six on the north section and saw the ape-

cies frequently in ones and twos all over the

south section, from the Cusuarina-clad ridge

to the sea-cliffs.

Nesting: At the north base of South Hill,

Pearson I,, we found an old fest in & crevice,

made entirely of mud, Mitchell & Behrnudt

found nests on Creenly and remarked on “the

far greater use of sheoak needles and other

orgamie matter in the nests of these birds on an

island where pood binding earth is absent"

Eckert (1971) reported nests from Franklin [

made mostly of fibrous material with no mud

apparent.

Anthus novaeseelandiae (Gmelin), Richard's

Pipit

In Febroury 1974 one was regularly seen

on the limestone plateau of the south section

of Pearson IT. (Hornsby 1978). The species is

eommon on Flinders f. (Bckert 1970).

Sericarnis frontalis (Yigors & Horsfield)

White-browed (Spotted) Scrubwren

On 16.11.1974 P, Martinsen tentatively iden-

tified a scrubwren of this group in thickels on

the upper slopes of the north section of Pear-

son J. (Mornsby 1978), There are no other

records from Pearson |, though the species is

common on Flinders 1, (Eckert 1970).

Megalurus pramineus (Gould), Little Grasshird

We encountered this species only on the

north section of Greenly, where it was Fairly

common on the shrub-clad slopes, Its (appa-

rent) absence from the south section of

Greenly may be attributable to grazing by the

Tammar Wallaby, which is pot present on the

north section,

In South Australia this species occurs mainly

in the eastern part, including Eyre Peninsula.

Although its occurrence on offshore islands has

not been appreciated, it has been recorded

from several: Waldegraye, Williams, Hopkins,

Reevesby, island in Pondalowie Bay, Trav-

bridge, Kangaroo, Bushy. Heatrice and Baudin

Rocks! (see also Whinray (1976) for nates on

its occurrence in the Furneaux Group, Bass

Stra).

199

Specimen: B30476, Greenly 1, {north section),

28,xi,L976, adult Male, testes slightly enlarged,

skull fully pneumatized, colours (immediately

ufter death): Jegs and feet flesh-grey, soles

creamy; iris brown, upper orandible with blackish

cilmen and pale cream tomia; lower mandible

creamy grey af base, dark eyey at tip, mouth

creamy flesh; eyerim grey; stomnch contents elytra

af small black beetles and othee chitinous frag-

ments. Collected '805 hrs in low shribs on rocky

hillside.

Taxonomy: Keast (1956) recognized two

mainland subspecies of M. grasineus: the

southwestern Mug. thomas’ Mathews and the

eastern and southeastern M.g, goulburni

Muthews, the former distinguished in being

darker above and having generally heavier

ventral striations than the Jatter, The specimen

from Greenly is faiyly davk above, but matches

specimens of Mv. gavlbure/ in the lightness of

its ventral streaking.

Petroica goodenavii (Vigors & Horsfield),

Red-capped Robin

Pearson I, Recorded all visits except 1914.

We found the species common in Casnarina

stricta? Woodland and jn the area of burnt

Melaleuca lanceelata-M) halmaturerum on the

forth secuon. Several pairs were attending

well-fledged young.

Dorothee J, In the nhsence of Casuarina and

Melaleuca uw presumably does not occtir

Greenly |, Noted by Finlayson (1948) and

Mitchell & Behrndt (1949) in Casuarina stricta

and Mfelaleuew lancealaia on ihe main ridge.

The latter authors found a nest with young.

We noted numerous individuals in the above

habitat, including several pairs feeding fledge-

lings,

Specimens’ (all collested 0945-1545 rs,

4.411976, north section, Peorsom 1.). 30477,

imm, fermale, solitary: gonads undeveloped, skull

fully pileutnaled. B30478, adult male, solitary;

fesles enlarged (7 reereasing), skull fully pnoumu-

tized. B30479, udule male, solitary; testes small,

skull fully pneumatized. B30480, udult male, soli-

tury; lestes enlarged (? regressing), skull fully

Pnecumatized; 830481, imm. rate, with adult

male-phase bird, calling a high seep seep seep;

testes minute, dome of skull largely unpneuma-

teed £39482. adult male, with adult female-phase

binl: testes enlarged: skull fully pneumatized.

30483, adult fernale, with adult male-phase bird;

oocvies Tegressed, oviduct dilated and convoluted,

large Wroodpatch on abdomen; skull fidly pnowma-

lized; possibly (he mother of B30481,

Colours of unfeathered parts (within 1) min of

death) =

200

Adult males; legs and feet blackish, soles cull

buffy yellow, bulty yellow or yellowegrey; iris very

dark browo; Upper miindible blickish; lower mur

tible blackish, some with rami ant basal tomia

horn or dull yellow: gape bully, dull yellow, dull

buffy yellow or orange vellow, south rich yellow,

dull ornge yellow, orange yellow, or dull yellow.

everin) black, blackish ur blackish brown,

Adult female: Jegs and feet blackish brown

(sules not notect); iris damaged; bill bluckish erey;

“ape yellow: mouth bright orafige yellow; eyerin

dark erey,

Tout). mate: legs and feet greyish blick. soles

ochreous bully iris dark brown, hill blackish

brown. pape: bully yellow; mouth deep bright vel-

low: cyerim blackish brown,

Imm. female! legs and toes black, soles bully

yellow: iris very dark brown: bill blackish hrown:

gape dull yellow, mouth orange yellow; eyerim

blackish brown.

Teronomy: Specimens collected on Pearson

J}, by us and by Cleland (1923) do not appear

to differ morphologically from specimens ol

the mainland populations. In our apinion, how-

ever, the song of the Pearson L. population is

distinctly different from that of miainland birds

(sang not heard on Greeny),

Pachyeephala pectoralis (Latharn), Golden

Whistler

Pearson L. only, Recorded on all visits except

1960 and 1973, Apparently confined to the

north seetion, where we found it fairly

numerous (and singing) in dense Casuarina

snivia and Melalenea lanceolata thickets.

Specimens: B30484, Penrson 1. (north sevtion)-

24,401976, ndult ferme, oovytes not enlarged

skull fully preumutized; colours (shortly afer

sleath): legs and feet pale greyy iris reddish, lipper

mandible black, lower mandible blackiwh: mouth

creamy flesh: eyerim bluckish. Calleered cu 1500

tirs in Casuarina stricta and oer scrub on rocky

hillside; slone-

R30485, Peurson I, (north section), 24,xi, 1976,

dull male, testes enlarged, skull smashed by shot.

colours (5 mins after death): legs and feet black-

ish, soles creamy: iris red: bill black; mouth

creamy Nesh; everia black, Cofleeted cv 1500 hres

in Caxnarina Attica and other scrub on rocky hill-

side; with another adullanale phase bird,

Tayonanyv: The populations of Pearson 1,

and Flinders 1. are referable to Pop. /uliginese

Visors & Horsfleld, af soythern Western Aus.

Iralin, southern South Australia (except the

lower South-East) and northwest Victoria,

This subspecies is characterized mainly by

females and vncoloured males having the

underparts buffy cinnamon,!

SHANE A, PARKER & JOHN BB. COX

Zosterops lateralis (Latham). Silvereye

Pearson [. Recorded on all previous visits,

The commonest passerine on the island, occur-

ring in small fiocks mainly on the north and

south sections, We noted it in dense thickets

of Melalenea, and in the chenopods and other

low dense shrubs og level graund and on the

houlder-strewn slopes,

Dorothee J. Noted as common by Paton

(1971), We recorded jt in snvall numbers ull

over the island, among low windswept shrubs

of the slopes and summits.

Greenly 1, Mitehell & Behrndt (1949)

reported jt as common on the south section,

favouring the stunted Melalevca lanceolita on

(he precipitous slopes and ledges below 76 m,

They noted several young birds incapable of

sustained flight, We noted it as common fram

sealevel to the ridgetop, mainly in Casnerina

stricta and M- lanceolata, with wv flock of ea 30

in a clump of Meuhlenbeckla adpressa, 1 was

alsa common on the north section in the dense

low ungriized shrubs on the steep slopes

Lichenostomus virescens (Vieillot). Singing

Honeyeater

Recorded only by Paton (1971), who saw

one bird on Pearson |, in January 196%.

Phylidonyris novachollandiae (\.atham). New

Holland Honeyeater

Mitchell & Behrndt (1949) recorded three

“somewhal bedraggled” individuals on Greenly

I, one of which they collected (SAM

B24768),

Ephihianwra albifrons (Jardine & Selby).

White-fronted Chat

Pearson bt, only, Cleland (1923) noted jt as

“one of the commonest birds on (he islands”

in January 1923, Recorded by Thomas &

Edmonds, January 1960 (Paton 1971), Paton

recorded u few small Mocks, eaeh of about six

birds, feeding mainly in the saltbush, and

banded an immature, whose conspicuous yel-

low gape suggested that the species had bred

an the island. We saw only one, a bird in

female plumoge, on bare granite boulders on

the south section: on being disturbed, it flew

out over the eastern bay,

Epbthianura tricolor Gould. Crimson Chat

Five noted en the northern slope of the

iurth seetion of Pearson I. an three consecu-

live days in January 1969 by Paton (1971),

BIRDS OF PEARSON, DOROTHEE AND GREENLY ISLANDS 21

Two small red-rumped birds seen flying out to

sea from the north section of Greenly 1. by us

Were almost certainly of this species,

Passer domesticus (\.innacus), House Sparrow

Cleland (1923) entered a “very doubtful”

sighting of two or three birds on Pearson L, in

January 1923, Paton (1971) recorded a flock

of ca 40 on the eastern point of the north sec-

tion of the island in January 1969, and a few

on Dorothee I. We recorded a few on the north

section of Pearsou, and two on Dorothee. Pos-

sibly the species is a vagrant from Flinders 1.

(Where it is very common) thal has so far

faved to establish itself.

Sturnus vulgaris Linnacus, Starling

Cleland (1923) recorded a small flock over

Pearson |., but added, “This record cannot be

considered as established beyond all doubt”,

Paton (1971) noted that the specics was os

nimerous as the House Sparrow (on Peyrson

L.), observing 20-30 at one time, including

many immatures, Hornsby (1978) noted one

or two birds on the middle section in 1973. and

1974. We noted two parties on the south xec-

tion of Pearson (one of 5-6, one of ca 30),

und tive lets on the north section (of 1, 10,

12, 2 and 3 birds). On Dorothee we recorded

four lois of 10, 4, 2 and 2? birds,

Artumus persanatus (Gould), Masked Waood-

swallow

Noted on Pearson I, only. Cleland (( 1923)

tenfatively identified two pale bluish wood-

sWallows as this species, Paton (1971) noted

one bird only, and referred to others seen by

Thomas and Edmonds ip 19@(, We saw a pair

on the fierth section in an area of Casuarina

yrefeta and burnt Afelalewee,

Corvus coronoides (Vigors & Horsfield)

Australian Rayen

Pearson ob Waite oted “erows' on

274.1914, und Wood Jones Found corvids

resiing in Cusuarina on 25,x1,.1920 (Cleland

1923). Cleland noted “some 30 of 40°) of

which he collected two adults and a subacute

(B4247-8, 28515). he also reported un ure

oecupled pest on the north section. Details al

the stomach contents of Clelund’s specimens,

which included vegetable matter. inseets and a

rat, Were given by Cleland (1923) and Lea

(1923),

‘Thomas and Edmonds noted corvids an

January 1960 (Paton 1971). Paton recorded

C. coronoides in January 1969, identifying the

species by ils call, She wrote “usually in pairs,

though sometimes as miiny us six might be

scen feeding toxether on wave-washed debris

on the rocks. ,,. An old nest, probably of this

species, was seen in a Casuarina.” Hornsby

(1978) recorded the species in 1973 and 1974,

on all three sections, the largest number ab-

served being 14. The birds were seen to pick

at crabs and small fish stranded by the tide,

und on one occasion several Were seen al a

freshly-dead Little Penguin.

We recorded the species mainly among the

high rocks of the north and south sections, We

estimated a maximuin of six birds, which

ranged regularly the length of the island.

Dorothee I. Paton (1971) recorded four.

We saw a party of three.

Greenly |. Finluysou (1948) noted under

Corvus spi “Two birds seen and more often

heard on the main ridge,” The following month

Mitchell & Behrndt (1949) noted seven cor-

vids roosting regularly in two large Casiitrind

Irces just below the summit of the south sec-

tion; these trees eontained several oests, only

one of which appeared to have had recent tse,

We noted a maximum of five C. coranvides

fidentified by their wailing call), along the

Cesvaring-clad main ridge,

The oceurcenee of the Australian Raven on

South Austriliun offshore islands has not been

fully appreciated, TL has been collected or reli-

ably recorded on St Franeis, Franklin [s.,

Flinders, Pearson, Dorothee, Wualdegrave,

Greenly, Thistle, Hopkins and Kangaroo [.,

and is probably the eorvid involved in sightings

on Spilsby, Wedge, and the South Neptunes.

The only island from which the Litthe Raven

C. mellor! has reliably been recorded is Kan-

earoo [!

Acknowledgments

We thank TP. J, Fatehen and L. Williams for

the wWentilication of plant material, and G. B.

Ragless, B. PMutchins, FP, Lewitzka and J,

Metcun for helpful advice in other matters.

SHANE A. PARKER & JOHN

B. COX

References

BepForp, W. R. (1972) Bird Talk 1, 3.

CLELAND, J. B. (1923) The birds of the Pearson

Islands. Trans. R. Soc. S. Aust. 47, 119-125,

Conpon, H. T. (1938) The birds of Reevesby

Island, Sir Joseph Banks Group, S.A. S. Aust.

Orn. 14, 187-192,

Cotton, B. C. (1960) Mollusca eaten by birds.

Ibid. 23, 44-47.

Cox, J. B. (1976) A review of the Procellarii-

formes occurring in South Australian waters.

Ibid. 27, 26-82.

Eckert, H. J. (1970) Birds of the Investigator

Group, with special reference to Flinders

Island. Ibid. 25, 201-205.

Farr, P. (1978) The significance of dropping be-

haviour in Pacific Gulls. Aust. Bird Watcher

7, 145-147.

Fintayson, H. H. (1948) Greenly Island, South

Australia, S. Aust. Orn, 18, 72-73.

Fritn, H. J. (1977) (ed.) Reader's Digest Com-

plete Book of Australian Birds, 1st rev.

(Reader's Digest, Sydney.)

Hornssy, P. E. (1978) Notes on the birds of

Pearson Island. §. Aust. Orn. 27, 280-284,

Keast, A. (1956) Variation in the genus Mega-

lurus. Proc. R. zool. Soc. N.S.W. 1954-55,

Lea, A. M. (1923) Stomach contents of Pearson

Island birds. Trans. R. Sac. S. Aust. 47, 361.

Lirrcer, F. M. (1910) A handbook of the birds

of Tasmania and its dependencies (Launces-

ton).

McKean, J. L. (1963) Lord Howe Expedition,

1962. Aust. Bird Bander 1, 84-90,

MitcHett, F. J. & BenRNbT, A. C. (1949) Fauna

and flora of the Greenly Islands. 1, Intro-

ductory narrative and vertebrate fauna. Rec.

S. Aust. Mus, 9, 167-179.

Parker, S. A. (1977) The distribution and occur-

rence in South Australia of owls of the genus

Tyto. S. Aust. Orn. 27, 207-215.

Paton, J. B. (1971) Pearson Island Expedition

1969. 6, Birds. Trans. R. Soc. S. Aust. 95,

149-153.

SERVENTY, D. L., SERVENTY, V. & WaARHAM, J.

(1971) “The Handbook of Australian sea-

birds.” (Reed, Sydney.)

STIRLING, I., STiRLING, S, M, & SHAUGHNESSY, G.

(1970) The bird fauna of South Neptune

Islands, South Australia. Emu 70, 189-192.

TarsurtTon, M. K. (1977) Nesting of the Red-

tailed Tropicbird at Sugarloaf Rock, WA.

Emu 17, 122-126.

Wuinray, J. S. (1976) The Little Grassbird in the

Furneaux Group, Tasmania. Aust. Bird

Watcher 6, 321-325.

Woop Jones, F. (1937) The breeding of the

White-faced Storm Petrel (Pelagodroma

marina) on South Australian islands. §. Aust.

Orn, 14, 35-41.

DEEP SEA FAN SEDIMENTATION OF THE KANMANTOO GROUP,

KANGAROO ISLAND

BY D. J. FLINT

Summary

The Kanmantoo Group sediments cropping out between West Bay and Breakneck River, Kangaroo

Island, are predominantly immature metasandstones with lesser metasiltstones and metamorphosed

lutites (schists). Lithologies and sedimentary structures show ordering in two distinct types of cyclic

sedimentation (sequence 1 and 2). Cyclic sedimentation units (1-3 m thick) are arranged in sets

(0.5-3 km thick) of only one cycle type. Vertical separation in the stratigraphic succession of the

cycle types into broader sets is a distinct and important feature. It highlights different depositional

processes.

DEEP SEA FAN SEDIMENTATION OF THE KANMANTOO GROUP,

KANGAROO ISLAND

by D. J. Fuinr

Summary

Fuint, 0.5, (1978) Deep sea fan sedimentation of the Kanmantoo Group, Kanguroo Island.

Tras. RK. Soe, S, Aust, 102(8), 203-222, 30 November, 1978.

The Kanmuntoo Group sediments cropping out between West Buy and Breakneck River,

Kangaroo Island, are predominantly immature metasandstones with lesser metusillstones and

metamorphosed lutites (schists), Lithologies und sedimentary structures show ordering In two

distinct types of cyclic sedimentation (sequence 1 and 2). Cyclic sedimentation units (1-3 m

thick) are arranged in sets (0.5-3 km thick) of only one cycle type. Vertical separation in

the stratigraphic succession of the cycle types into broader sels is a distinct and important

feature. Tt highlights different depositional processes.

Sequence | deposits have a relatively limited variety of sedimentary structures, und ure

characterised iff part by 4 thick massive sandstone base and lutite top. Sequence 2 deposits

contain a very wide variety of depositional und syndepositional deformation structures. within

predominantly metasandstones, Medium scale foresets are abundant in areas of sequence 2

units, but occur randomly within these units, Both sequences are interpreted to have been

deposited from (urbidity currents with a bed load phase, but exhibit strong differences in the

relative importance of traction and fallout processes.

The sediments are interpreted to have been deposited in a middle fan environment, ie.

channelled suprafan and suprafan depositional bulge. The size, abundance and random posi-

rioning of foresels makes these Very unusual turbidite deposits,

Introduction

Kanmantoo Group metasediments cropping

out between West Bay and Breakneck River,

Flinders Chase, Kangaroo Island, South Aus-

tralia (Fig. 1) were examined to determine

their depositional, structural and metamorphic

history, Structural and petrographic details are

discussed jn Flint & Grady (in press). Sedi-

mentological uspects were investigated to deter-

mine mode and environment of deposition,

transport processes, pretectonic orientation of

pulaeocurrents and palaeoslope and possible

provenance.

Previous work in Flinders Chase is limited.

The regional geology of Kangaroo Island was

established by Wade (1915), Sprigg (1954),

Daily (1956). Thomson (1969) and for Flin-

ders Chase hy Major & Vitols (1973). They

concluded that during the Cambrian, when

Kanmantoo Group recks were being deposited

the sea floor in the position of Kangaroo Island

“School of Earth Sciences, Flinders University of S. Aust,

area subsided (Waitpingan Subsidence) syn-

chronously with uplift (Cassinian Uplift) of

the Gawler Craton to the northwest. Grey,

medium to coarse grained greywackec-arkoses

with sharply truncated crossbedding to 1 om

high, scour channels and slump folds typify

the Kanmantoo Group rocks cropping out in

Flinders Chase (Major & Vitols 1973), Slump-

ing is in the same direction as the dip direc-

tion of forescts, With a westerly source indi-

cated. Lack of sorting, abundant submarine

slump structures afd sudden thickening across

fault hinge zones Were inlerpreted to indicate

rapid transport and sedimentation with violent

downward movements of the sea floor during

sedimentation,

To Flinders Chase, Kanmantoo Group rocks

examined here are exposed along 8 km of

coastline in a strip often only 20 m wide from

sea level to clifftop, Inland, Quaternary con-

solidated aeolian limestone, with minor piso-

Bedford Purk, S$. Aust, 5042. Present

address: Geological Survey of South Australia, 191 Greenhill Road. Parkside. S. Aust. 5063.

24 D. J. FLINT

FLINCERS /-CHASE~

: HA

‘ aw

v NATIONAL ATPARK

mis A ’

-# wt

Crag FO ROOKY RIVER”

“ ons

AILDMETRES

Dy fl) Sacto

Tht Lib

Fig. 1. West Bay area, Kangaroo Island.

5 1A TE Decentmnet avis eed Een ey

litic laterite and siliceous sands, blanket the

older rocks. The Kanmantoo Group comprises

predominantly quartz-rich metasandstones,

melalutites and quartz-mica schists, with less

abundant types being pelitic and biotite-rich

lutites, calc-silicate boudins, and actinolitic,

biotite-tich and heavy-mineral-nch sandstones.

Most rocks are quartz-rich (to 30% by vol)

and argillaceous (now recrystallised to biotite

and muscovite), A very Wide Variety of btrac-

tion, liquelaction, collapse and syndepasitional

deformation struciures are developed. Lithi-

fication prior to regional deformation and wely

low pressure mlermediale Facies metamorphism

during the lower Ordovician (Dasch et al.

1971; Milnes e¢ al. 1977), have preserved

many Sedimentary structures,

This report describes and mterprets the sedi-

mentary characteristics of the Kanmantoo

Group, so interpretive rock oames such as

lutite, siltstone and sandstone are used, even

though the rocks have been metamorphosed

to the andalusite-staurollte zone of the amphi-

bolite facies (Flint & Grady in press), As the

precise depositianal processes and transport

mechanisms are very interpretive, non-genetic

terminology (sequence 1 and 2 units) has been

adopted for the two distinct cycles of sedimen-

tation exhibited. A Markov analysis technique

is used fo illustrate statistically the sedimentary

cycles present, Sequence 1 and 2 units occur

in separale intervals af the succession and are

not interbedded mesoscopically (Fig. 2). This

type of sedimentological analysis involving

Markov modelling represents (he first on Kan-

mantoo Group sediments.

Sequence 1 deposiis

Deseription

Deposits of sequence | units consist of con-

secutive cycles of upward fining units with a

massive homogencous basal sandstone and a

lutite upper portion (Fig, 3, Traverse A).

Within each unit variation of grain size is

gradational and the basal contact with the

underlylig Iutite (now quartz-mica schist) is

sharp and planar, except where tectonically

deformed (Figs 4-5), Units vary in thickness

from 0.1 m to 4 m (average approximately

{ m), Sandstone to lutite ratio averages 11

and the greatest uninterrupted massive sand-

stone interval is 80m. The major sedimentary

structures observed within sequence 1 deposits

are ellipsoidal intraclasts, small scale ripple

cross-stratification and small slump breesias,

rare load and flame structures, ripped-up clasts

and sandstone dykes and sills. ‘Teetonism and

metamorphic differentiation have destroyed

nearly all of the sedimentary structures within

the lutites (Fig. 5).

Intraclasts are ellipsoidal quartz-rich sand-

stones with maximum axial lenuths of 0.25 and

0.15 m and oriented with the long axes parallel

to bedding. Clasts oceur throughout the lower

half of the units. Siniilar clasts are deseribed

by Stauffer (1967). Fisher (1971), and Hamp-

ton (1972)-

Slump breeciay oecur near the top of many

massive sandstone divisions and consist ol

stall elongate sandstone clasts in a sandstone

matrix (Fig. 35), Clast orientation is now

related to tectome structures and Flint &

Grady fin press) conclude from differential

states of strain in deetonic structures, thar

transposition of sedimentary layering was peue-

contemporancous with sedimentation. Re-

orientation of the transposed bedding occurred

during tectonic deformation,

Small tipple cross-stratification and plane

parallel laminae are observed us thin divisions

above the slump hereeeias and near the centre

of many units. Below, sandstones are massive,

while above, former lutites are extensively

folded, crenulated and differentiated,

Rarer structores m sequence 1 deposits are

load casts und sandstone dykes and sills. Sand-

stone lobes (load casts) into underlying lutite

are developed where the lutite has been pre-

served, Load casts are cither symmetrical, pos-

sibly indicating formation after deposition of

FAN SEDIMENTATION—KANMANTOO GROUP 205

LOCATION OF TRAVERSES

SEQUENCE 2 DEPOSITS

Upward and downward fining units

VERY SHARP

PELITIC LUTITE = —— — = TRANSITION

SEQUENCE 1 DEPOSITS

Upward fining units

Sequence fines and thins upwards

WEST BAY

EROSIONAL

CHANNELLED

SURFACE

SEQUENCE 2 DEPOSITS

Upword and downward fining units

Sequence coarsens and thickens upwards

GRADATIONAL

-b

PELITIC LUTITE ; ==" ZOUNDARIES

SEQUENCE 1 DEPOSITS

Upward fining units

Sequence fines and thins upwards

KILOMETRES

| 2

LEGEND

STRUCTURES LITHOLOGIES

[ Climbing ripple : Poorly sorted, medium

= cross—stratification fo coarse grained

sandstone —_ 2

Poorly sorted, fine

Extraformational grained sandstone — __

Parallel lammation —| conglomerate Lutite, often biotite =]

Intratormational rich

Tabulor cross—bedding SS iranspased bedding. — Gemere|

ae Conglomeratic sundstond_ Cabo

SLUMP STRUCTURES TS] Heavy mmnerol—nch im

je ra sondstone — ——

Trough cross—bedding Slumped foresets

BED BASE TYPES Slumped massive, [lat

Transitional 9 edded and poorly

bedded sandstones __ i 1

Abrupt Convoluted lutite ~ : Silt and clay Fine, prediugy ard

Erosionol — siciceee or sandstone _ ——s—_EE } Soaeerson

GRAIN SIZE

77-74 DJ. Flint Geoloais| S.A Depatimen! of Mines

Fig. 2. Distribution of sequence 1 and 2 deposits and pelitic lutites in the West Bay-Breakneck River

area, Note lack of mesoscopic intermixing of deposit types. Legend for and location of litho-

logical logs in Fig. 3.

206 D. J. FLINT

VERTICAL SCALE

METRES

ALL SECTIONS

FACE NORTH

Bd, Flint Geolagist S.A. Department of Mines

Fig. 3. Observed detailed lithological logs for sequence 1 deposits, transitional pelitic Iutites and

sequence 2 deposits.

FAN SEDIMENT ATION—KANMANTOO GROUP 207

the sandstone, or asvmmuetrical, suggestinut syn

depositional deformation. Injected laminated

lutiies between sandstone lobes resemble Mame

structures. Load cast height is invariably less

than 7 cm. Small sandstone dykes and sills are

observed in only one locality and consist of

massive coarse sandstones of similar grain size

to sidjacent massive sandstones, Sills (fed by

the dykes) are discontinuous, while the dvkes

have an orientation similar to slump fold sxial

planes, suggesting that dyke formation is along

a plane of weakness formed by downslope

penecontemporancous ercep,

Thinly laminated to massive sulphide-rich

and actinolitic sandstones occur sporadically

helween sequence | unis, They comprise less

than 1% of the total thickness of all seyuenve

| deposits

Process of depesition

The sequence of thick massive sandstone

division al the hase, followed progressively up-

wards by a thin division of rippled wid fami-

nated fine sands and sills, and then a thick

lutite division correlates well with Bouma's

“acde" sequence (Bouma 1962), The sediment

In sequence | Units is interpreted to have heen

transported by turbulent mass flows with u

hasal sand slurry flow.

The first phase of deposition appears to be

Irom rapid seitling of grains oat of suspension.

probably as a “quick bed” from a basal slurry

flow to the turbidity current) the mechanism

of quick hed sedimentation is as outlined in

Carter (1975), Walker (1976) und Rust

(1977). Occasional lasts are trapped through-

out these beds, and there presence in other

deposits at various levels has been related to

a linite yield strength of the slurry flow

(Hampton 1972). Near the top of many “a”

divisions are slump breccias which are pro-

bably related to mass shearing and dewatering

during consolidation. This interval may once

have had diffuse parallel lamination and equate

to Bouma’s “h" division, “Streaked-out lami-

nac” have been described in a similar setting

by Skipper & Middleton (1975) hit their

example involves more plastic syndepositional

deformation, This basal division of missive

sandstone, with scattered clasts and diffuse

lamination, has many similarities to grain flows

and debris flows of Stauffer (1967), Fisher

(1971) and Carter (1975).

The finely rippled and laminated division

near the centre of most units is correlated

with Houma's “ec” division and lower low

regime currents. When present, it is always

thin and aecerding to Walker & Mutti (1973)

4“ common observation is that the greater the

number of sequences which begin with

Boumas ‘a! division, the more uncommon is

parallel and rippled lamination within those

units.

The lutites at the top of each unit are often

of comparable thickness to the basal massive

Stuitdstones; these units are equated with the

normal graded beds of Corbett {1972}, Sedi-

memolowcal analysts of structures within these

lutites 1s limited due to extensive development

of folds and other tectonic structures, includ-

ime new differentition Sayerings (Fig, 5),

Deposition fram waning, ow velocity currents

in the dilute tail of the turbidity current is

interpreted as the likely depasitional made,

The sedimentation process for sequence |

unis is interpreted to be rapid deposition from

waning currents. In this way, few traction

structures Would he developed, with the sedi-

ment being tried as soon as it is deposited.

‘Transportation of the sediment is as 4 turbu-

lent mass flow with a basal hed flow (slurry

flow)

Transitional Infite deposits

Developed ahove intervals dominated by

sequetice | usits are two pelitic lutites iq 30m

thick (Pig, 2), Parallel lamination is the domi-

nant sedimentary structure (Fig. 6) and rare

structures are pseudouodules, sand ripples and

thin (less than 1 cm) sand. sheets (Fig, 7), In

pelitic futile has gradational boundaries both

with the underlying sequence 1 deposits and

overlying sequence 2 deposits. These lutite

intervals are Iransitional between the thick sets

of cyclic sedimentation units.

The [two pelitic [utite intervals indicate

periods gnd/or areas of relatively quiescent

sedimentation, Sand ripples, thin sand sheets

ald predominantly clayey silt’ sedimentation,

suggest deposttion and reworking from slow

moving curtents with a low sediment concen-

tration.

Sequence Z deposits

Deceriptlow

A wide Variety of sedimentary structures

ure observed m sequence 2 deposits m contrast

to their relative scarcity und lack of variety in

seqnence | deposits. Structures developed are

hedding (massive. plane parallel, slumped and

208 D. J. FLINT

ia: AREER 8

Fig. 4. Several sequence 1 units occurring in upper portion of interval of sequence 1 deposits, with

single phase deformation at a low angle to bedding. Pen for scale 13 cm long.

Fig. 5. Several sequence 1 units strongly deformed in lutite portions; most common style in outcrop.

Note slump breccia above the upper massive sandstone bed.

FAN SEDIMENTATION—KANMANTOO GROUP 209

- . _-

imeaiilh i alia, 2.

r™«... J iets

Fig. 7. Rippled sands and a thin disrupted sand bed within lutites of transitional lutite sequence.

. ’ a

Y - 4 in ”

210 D. J. FLINT

BP FIG 9

Fig. 9. Very thick interval of superimposed foreset divisions in a 40-m cliff-face, north side of West

Bay: sequence 2 deposits.

D. J, FLINE

convoluted), cusp structures, oriented clasts,

climbing ripple croés-stratification, small dia-

pir-like fealures and Irquefaction structures.

The rock types are preclominanily medium to

coarse grained, imimatufe quartz-feh sand-

stones ‘with concentrations of giream (Flint

1976).

Observed sequences. of lithologies and struc

tures are shown in Fig, 3 (Traverses D to H)

and Fiy, 8, and have been subjected ta Markov

analysis.

At or near the base of many sequence 2

units are massive to poorly bedded, pourly

sorted sandstones which have un average thick-

ness Of 1.3 m (0.11-4.25 i) they represent

35% of the total thickness of sequence 2

deposits, Clusts are o¢ensionally present im this

sandstone type, and their ovientation varies

from parallel to croded base to imbricated with

clasts dipping in the direction of flow, Clusts

are consistently léss than QO.) my long and pre-

dominantly of biotitic Ivtite, Near the hase of

many units (bui above the niassive sandstone

divisions) are coarse, fiat bedded sandstones

which form the most common lithology, hath

in the number of beds present and total thick-

ness (40% of sequence 2 deposits), ‘Thickness

of individual flat bedded sandstones averages

0.9 m (0,18-4.60 m),

Foresets and inclined strata represent 12%)

of the total thickness, have an average thick-

ness of 0.5 m (0.03<1.8 m), Most foresets

are distinctly tabular with usymptouc foreset

bases and sharply truncated tops. In profile,

tabular foresets vary thom lensing Out over 4

few metres, Lo conliminus aver 50 m but with

gently undulating upper and lower hounding

surfaces (Fig: 9), Some foresets are trough

shaped and deposited in asymmetrical scours.

up to 2m deep, with steep upcurrent sides.

while the downcurrenr depositional surface is

nearly tangential to bedding. With that part

of the stratigraphy of only sequence 2 wnits,

toreset development varies considerably [ror

small intervals of no foresels to intervals of

abnndant and superimposed foresets (Fig, 9)

The extent of foreset development has uo is-

cernible relationship with anv other charac-

teristic of sequence 2 Units Tntraformational

recumbent folds with axial plines parallel to

bedding are developed from shemping of fore-

sets (Pig, 10). Identical structures are reconiest

in Pettijoho & Potter (1964. plare 110) arid

have been observed elsewhere within Kan-

mantoo Growp sediments in Flinders Chase

(Major & Vitols 1973), Selective slumping 75

rau

common, with ouly a few i a succession of

foresets being slumped, Partial slumping within

individual foresets also occurs, with a marked

tendeney for humogeuisation towards foreset

tops,

The upper portion of many intervals consists

of either massive or finely larninated lutte,

with alternating biotite-rich and quartz-rich

layers. Lutiles represent 11% of the total

thickness of sequence 2 deposits, and have an

average thickness of 0.4 m (0,02-1.64 m).

Heavy-mineral-rich sandstones (less than 0.1%

total thickness) are commonly developed

above the laminated lutite und exhibit grada-

himal contacts. Banding within the heavy-

minetal-rich sandstones is comprised of alter-

nuting lavers (mm thick) of quartz-tich and

lieavy-mineeal-tich sandstones and tutites,

which grade up into a massive, heavy-mineral-

rich Wpper portion. Laterally, lutites and over-

lying heavy-ermeral-rich lutites are lenticular,

and wre truncated by the next sechmentation

until.

Slumped and convoluted bedding is ubiqui-

lous tor wll af the areas characterised by

sequence % deposits. Slumping of whole

seyiiences Of strictures is more common than

convolution of single beds.

Hiehly chaotic slumping with continuity of

layering is typical (Fig, 11) and folds vary

in Style through plapar-cylindrical to cusp-

shaped. In some maslances, contorted hedding

sugeests collapsed megaripples. Vertical thick-

ness Of slump-felded bands ranges from a few

centimetres to 6 om,

Rare dlapine structares ta 0.15 m high, and

liquefyetion structures felutriation columns of

Corbett, 1972) are observed in sandstones con-

faining slumped bedding and cusp structures.

Liquefaction features have developed fram up-

ward and downward movement of parallel bed-

ded sariistones, Resullant structures melude

disrupted domes, and sinking “teardrop”

shaped sandstones in # homogeneous tmatrix

(Figs 12-13). Simitar small diapirice structures

(fuotured layering) in Japan are deseribed by

Nagahama er al. (1975).

Lateral variations of lithologies and struc-

hires afe observed even Within the narrow

exposure limits of only 20 m-. Massive, poorly

bedded and flat bedded sandstones are

severally laterally continuous. hut foresets and

laminated funites offen thin and lense out

Iwterally. Downetirrent fiping is noticenble in

soe exposures, With foreset sandstones erad-

ing to climbing nipple crass-stratification or

D. J. FLINT

212

> ¥

Fig. 10. Overturning of upper portion of foreset laminae is very common, and produces intrafolial

folds, sequence 2 deposits.

Fig. 11. Chaotic hydroplastic slumping within sequence 2 deposits is prevalent: example from a

layered, fine-grained sandstone.

FAN SEDIMENTATION—KANMANTOO GROUP 213

mclined laminated Jutile, Small channels (ess

than 1m wide and 0.15 m deep) are filled with

massive or finely laminated lutite.

Markov analysis

Observations suggested that sedinventation

within sequence 2. units involved cycles of

jithologies and structures. To test the hypo-

thesis of cyclic sedimeutation, statistical testing

methods (Markoy analysis) were used, The

technique of Markov analysis in its applica-

tion to illustrating sedimentation cycles is out-

lined in Gingerich (1969), Krumbein (1967)

and Krumbein & Dacey (1969) and Pellijohn

et al. (1972).

‘Vests are mad¢ to prove whether a depen-

dence exists of one lithology or structure on

the previously deposited lithology or structure.

Two types of observational methods were

adopted:

I, Recording lithologies and structures at a

tixed interval of 1 m,

2, Recording transitions at Iithologie con-

facts and wherever sedimentary structures

vary.

Some of the divisions used i the latter method

are illustrated in Fig, 14.

Although the units have been modelled as

for 4 Markov process, the original sedimenta-

hom process may not be Markovian, ie, may

not have a built-in memory. Krumbein (1967)

outlines statistical criteria for testing the null

hypothesis.

The greatest thickness of uninterrupted ex-

posure Was chosen and consisted of 179 m of

sequence 2 deposits. It Was found that

sampling al a fixed interval of | m generates

random sequences of lithologies and struc.

tures. The same 179 m traverse was subjected

to another Markov analysis by noting all transt-

lions of lithology and structure. Results of this

analysis are tabulated io Fiys 15-16. The

sample statistic to test the null hypothesis, cal-

culated from the N Jn P matrix, is 150.2 which

is greater than the tabled Chi-square value for

36 deprees of freedom at the 0.05 level of

confidence, The hypothesis of an independent

trials process for sedimentation within sequence

2 units is rejected.

The sequence of structures and lijhologies

can be extracted from the probability differ-

ence matrix (Fig. 16). Those transitions with

positive entries have a higher than random

prohahility of occurring. ‘The cycle extracted

from the probability differenve matnx is ARE:

Transition Prebabiliy difference

A-B 0.29

B-E 0.08

E-A O03

The cycle does not contain the foreset beds

exists for transition up into fareset phase; how-

ever, once in the foreset phase, a high pro-

bability exists for passing up into lammated

luftle ¢2) For the 179 m traverse, the

sequence A BE is observed |i times and the

next most frequent sequence is A BCE three

limes.

Amalgamation of sequence 2 units appears

to be very common Which is in marked con-

trast to sequence | units, The complete

sequence (ABE) is observed only 11 times

because of amalgamation and the random dis-

(nbution of the foreset division.

The number of observations in this. strati-

graphic interval on bed types F and G are too

restricted to allow meaningful interpretations

of their relationships to other lithologies and

rock types.

Examination of the observed profiles for

sequence 2 deposits (Fig. 4) indicites that up-

ward fining and upward coarsening units exist.

However. observed profiles and the Markov

analysis reflect the dominance of upward fining

its. A unit based of average bed thicknesses

would be 2.6 m thick, The fully developed

eyele and fureset beds (A, B, C, & B) total

96% of the total thickness of sequence 2

deposits (Fig, 15),

Where seditnentatiun produced inclined bed-

ding, Vertical sequences (ABE) are also

observed faterally,

Palueaslope and palaeocurtents

Streaming lineations on flat bedded sand-

stones [as jllustvated in Conybeare & Crook,

1968, Plate 80.4) and foresets vive a down-

current direction concentrated in the range

OLS" wy 135° (Fig. 17). Fold axes and axial

planes of slump folds suggest a pretectonic

palacoslape dipping towards 115°.

No current directions or slump folds were

measured in sequence 1 deposits or the tran-

sitional litite deposits. Rare ripples and slumps

are Observed but are strongly tectouically de-

formed. All palaeocurrent and polaeoslope esti-

mates are from sequence 2 foresets, flat bed-

ded sandstones, latiinated Jutites and their

sluntped equivalents, Bedding, normals tn these

lithologies are distributed about a fold axis

plunging borizontally towards OT9° true north

ae ae r

<7)

D. J. FLINT

—

‘shee eee

et a 2 oe

FAN SEDIMENTATION—KANMANTOO GROUP

(Flint & Grady in press), Single axis rotation

was performed until bedding became hori-

vontal.

Slumping is assumed to be largely down the

palaeoslope so that slump folds developed have

axial planes striking along the palaeoslope,

Slump fold geometry stnctly reflects the

palacoenergy slope; bere the two slope types

are assumed to be equivalent

The spread of current directions may be

from single or multiple source flows. If a

+ 15° error is assumed in accuracy of palaeo-

slope determination, then 90% of palaeocur-

rents indicate flow in y 90° are between down

the palaeoslope and along the palaeoslope to-

wards the northeast, The lurgest concentration

of currents is north of the assumed palacoslope

direction. Differences in current directions were

not observed to be related to variation in litho-

logy, structures, or their spatial relationships.

Procesy 0] deposition

The fully developed cycle in sequence 2

units, as developed from the Markov analysis,

is compared with the idealised Bouma turbidite

sequence (Bouma 1962). Divisions “a”, “b”

and “d" of Bouma and their ordering ure the

same as sequence 2 units in Flinders Chase,

Although both sequence 1 and 2 deposits are

interpreted toa be turbidites there are distinct

differences between them: the strong difference

in the development of a thick well bedded “b”

division, the abundant foresets and the much

thinner “de” divisions of sequence 2 units.

Similarly to sequence | units which also start

with the massive “a’ division, Bouma's “c”

division of ripple cross-lamination is almost

entirely lacking in sequence 2 units.

Massive and very poorly bedded sandstones

at the base of many units represen! rapid depo-

sition from the bed load (slurry low) of the

turbidity current, and are analogous to

sequence 1 slurry ows. The flat bedded sand-

stones differ from the usual diffuse horizontal

parallel laminated sandstones in many turbidite

descriptions (¢.2. Bouma 1962; Walton 1967,

Walker 1967) in that the bedding planes are

215

strongly developed, sharply defined and spaced

several centimetres apart, These flat bedded

sandstones appear to represent transition from

bed load conditions to fairly uniform, upper

flow regime velocities. The average and muxi-

mum bed thickness of 0.9 m and 4.6 m re-

SYMBOLS

Mowive to poorly Wedded coprse gegined

hone wane

Coarse Hot bedded Wanditone

pots bedded sondélone aad inclined

shot

Conse gtod yardstanes

hor indled, oleenaiing biotte teh aad

quartz ach loyered lute

deovy mien! neh sandslones

Ripple lute

TOTAL PERCENT

THIGKNESS qT

\METRES) THICKNESS

as: 4s i"

NUMBER

BEOS

AVERAGE BED

THICKNESS

(METRES)

ta)

a 4

TOTALS q Kh we

TRANSITION COUNT MATRIX

OBSERVATIONS Al LITHOLOGIE CONTALTS

OL link eologel 5a, Oepartment af Aras

Fig. 15, Symbols and observations at lithologic

conlacts for the Markov analysis, se-

quence 2 deposits, Note for each of the

divisions, the average bed thickness and

percent of total thickness.

Fig. 12.

Syndepositional liquefaction structure with collapse and disruption of sandstone beds pro-

ducing tear-drop forms, sequence 2 deposits,

Fig. 13.

stone, sequence 2 deposits.

Fip. Ja,

Syndepositiongl liquefaction structure with disruption and upward doming of layered sand-

Some of the divisions used in the Markov analysis; poorly bedded sandstone, overlying lami-

nated biotine Jutite. overlying convoluted sandstone; sequence 2 deposits, Pen for scule 13

em Jong.

216 D. J, FLINT

spectively for these beds and their abundance

(40% of total thickness) illustrate [hal these

conditions were common, and that the current

decay was very slow,

Cross bedded sandstones und inclined strata

are @ very important phase of deposition.

Markov analysis strongly suggests that the

foresets do not occupy a fixed position in

sequence 2 Units, but occur randomly through-

out (the cycle and are overlain by layered

lutites. Thomson & Thomasson (1969) estab-

lished a sequence of “a-dunes-bede” for cal-

careous turbidites in the Dimple Limestone

(Texas). Walton (1967) and Allen (L969)

indicate that, based on studies of current velo-

cities and their decay, medium scale forests

could form but the structures recorded in tur-

bidites depend strongly on the rate of decay

of the turbidity current, The general absence

of foresets in turbidites is an indication that

currents apparently decay too rapidly.

The foresets represent a stable, aggradational

bed form which probably formed from sand

dunes (averaging 0.5 m high) migrating down-

current. Flat bedded sandstones grade into

INDEPENDENT TRIALS MATRIX

6 a t f

oul aw)

(I iF

{)! wy

yl 09

Wy) |

ro v

—

PROBAUILITY DIFFERENCE MATRIX

erable breernedepenmlent Hratl probatahty)

raph

eth i”

N inf MATRIX

Sue feet for geplereton!

Enmbote cdeliiwd mi basis

GASEPVATIONS AY UIHOLEGIC CON iacys

z ienlew 4 KA Gaucrtmenn rh Mine

Fig, 16, Mafkoy analysis of data presented in Pig

15. Sisnificant transitions ure those with

A positive entry in the N InP matrix.

cross-bedded sandstones Via low angle inclined

strata. The close telationship of these bed-

forms was also observed by Corbett (1972) in

u proximal flysch sequence, Tasmania, Fore-

set divisions apparently represent deposition

from sediment laden currents maintained Ut a

constant Velocity in the upper portion of the

lawer flow regime (from the bed form-flow

regime studies of Harms & Fahnestock (1965)),

As the flat bedded and cross-bedded sandstones

represent 52% of the total thickness of all

sequence 2 deposits, then the currents were

consistently at velocities transitional lo the

upper and lower flow regimes. Conditions of

uniform flow with a slow rate of deposition

ate known from turbidites (Middleton 1969;

Blatt et al. 1972) and Jead to units with trac-

tion structures. Mutti (1977) also indicates

that foresets represent traction processes ‘with-

out substantial fallout. The extent of turbu-

lence within these currents is problematical;

Sanders (1965) suggests that turbidity cur-

rents will not give rise to large scale traction

structures while Walker (1967) concludes that

foresets represent fully turbulent flow,

The flat bedded and cross-bedded sandstone

divisions are overlain (statistically) by flat

bedded lutites without the development of

small ripples. The thinly bedded hiotite-rich

and quartz-rich lutites indicate deposition from

the final waning stages of the turbidity current,

Heavy-mineral bands at the top of some units

with interbedded qvwartz-rich and heavy-

Miineral-rich layers, show that currents con-

lived to flow after sand and lutte deposition

at velocities sufficient to winnow the litite

fines wnd redeposit heavy minerals, A varicty

of curent lypes are possible for these deposits.

including oceanic contour currents, tidal cur-

rents or the tail of turbidiry flows. Middleton

& Hampton (1973) postulute a dilute et

trained layer which flows after the turbidity

curent body and reworks upper portions of the

turbidite deposit, and this is considered the

most probable explanation for the heavy-

Mineral concentrates, These concentrates have

significant differences to those attributed tf

deposition from contour-following bottom cur-

rents of Bouma & Hollister (1973, Table 1).

Contourite concentrations are supposedly as

placers in small scale stratification within

laminated silt and clay deposits, whereas con-

centrates of sequence 2 deposits sre often mas«

sive. not \issociated with ripples, always within

sandy seauence 2 deposits rather than |utites

and involve beth winnowing and redeposition

FAN SEDIMENTATION—

of heavy minerals. Traction, pulsating currents

causing lenticular sands with laminae of heavy

mineral concentrations have been observed in

vehicle dives and measured in current meters

(Shepard et al, 1969) at La Jolla submurine

canyon and fan valley, California.

Upward fining and upward coarsening jndi-

vidual units indicate the abundance and pul-

suling nature of the currents. Thomson &

Thomasson (1969) and Walker & Mutti (1973)

state that the order of occurrence of Bouma’s

divisions is very rarely inverted, bul Glaister

& Hopkins (1974) interpret units with grada-

uonal upper and lower contacts as represent-

ing continuous deposition from pulsating tur-

bidity currents.

Lateral lensing and wmalgamalion — of

sequence 2 units is very common and, along

with observing vertical sequences laterally

over u distance of metres to lens of metres

when the strata are inclined, suggest that the

depositional surface was channelled, or at least

had an uneven topography. J! the tulite divi-

sions originally were thicker, then preservation

of them to only 11% of the total thickness

(Fig. 15) would result from amalgamation of

sequence 2 units.

Environment of deposition

Water depth during sedimenotition is difii-

cult to estimate for a succession dominated by

turbidites, Calesilicate Mineralogy tn sediments

deposited between turbidites during periods of

relative quiescence, suggests deposition above

the contemporary calcite compensation depth

No structures are observed to indicate depo-

sition above the storm wave base,

Turbidites have been described from many

environments, but a thick turbidite succession

is most likely to be preserved in an area of

consistently deep and quiet water (Walker

1976). The succession of sequence | and 2

deposits is compared with models for deep sea

fans and sandy tectonic delta complexes. The

preceding sections have established that both

Sequence | and 2 units were deposited from

waning turbidity currents with a substantial

bed load component but substantially different

rates of deposition and current decay rates, A

distinctive feature is the perfect spatial separa.

tion of the two types of turbidity deposits.

Deep sea fans

Where observed (Fig, 2) the intervals of

sequence | deposits thin and fine upwards, and

have a thick massive sandstone hase up to 80

KANMANTOO GROUP 217

PRETECTONIC

ORIENTATIONS

4) CUARENE DINE ()ahas

PERCENT

12 SLUMP FOLG AXIAL PLATES

(NORMALS,

LOWEN HEMISPHERE

CQOUAL ARPA

PRCUEO TIONS

33 SLUMP FOLD ANES

Patel

PENIN Gb

epvt

FILOME I Hts

SA Dhagertiwint eat Mirren vi) Ever

_ Palucocu/rents and pretectonic slump

told geometry, and their relationship to

the inferred palaeogeography of Thom-

son (1975).

218

m ttck directly above a scoured, erosive base,

This style of apward fining and thinning of

scqyvences. dominated by Bouma “a” divisions

is Widely recognised as sedimentation in deep

sea fan valleys or channels (eg. Nelson &

Kulm 1973; Middleton & Hampton 1973;

Ricer-Lucely 1975) Rust (977; Walker 1977)

The massive, structureless sands al the base

of the succession are interpreted to be from

rapid deposition fram mass flows of high sedi-

ment concentration and low turbulence (Rust

(977), to amalgamation from channel mean-

denny (Walker 1976). Sequences dominated

by “ac” divisions are found in channels from

upper to lower fan environments (fHaner

1971), but vary from “a” division predo-

ininuting in upper fan channels to “e" division

dominant and with base cut-outs in lower fan

channels. The niost complete “ae” units are in

middle: fan channels or lower reaches of the

upper lan valleys (Nelson & Kulm 1973; Nel-

son & Nilsen 1974). Inner fan deposits usually

vonsist of large lenticular channel sands within

thick mudstone sequences (Mutt) 1974, Walker

& Mutt] 1973), but in the West Bay area they

are surrounded by a succession of sandy

sequence 2 dcposits. It is concluded that

sequence | deposits in Flinders Chase repre-

seut sedimentation in a channel of the middle

fan (suprafan).

Transitional lutite sequence developed at the

top of the charmel fill deposits may represent

interchannel sedimentation, a levee facies or

deposition from contour-following bottom cur-

rents, Well developed levees are known to exist

along decp sea channels and fan valleys (e.g.

Shepard & Murshall 1949; Piper & Normark

1971, Nelson & Kulm 1973) and contain

laminated silts and muds with a few thin sands,

very similar to the lutites above the successian

of sequence 1 deposits. If a middle fan environ-

ment is correct, then deposition from oceanic

hottom currents (deposits asx described in

Hubert (1966) and Bouma & Hollister

{1973)) is unlikely, as the current’s driving

mechanism 1s insufficient fo drive at well up the

slope of the depositional basin, A levee Facies

or iuterchannel deposition is concluded for the

transitional lurite sequences.

Sequence 2 deposits sre artanged mm a chick

upward coarsening and thickening set: this

stwle of deposition js most often interpreted as

f prograding depositional bulge on a deep sea

fan (eg Walker & Mutth 1873. Nelson &

Kulta 1973. Mutt) 1994: Ricei-Lucchi 1975;

Walker 1974). The unusual feature of

D. 3, FLINT

sequence 2 deposits are the foresets which

figure rarely in descriptions of turhidive depo-

sits, with Potter (1967) Tsting large scale

cross-beds as characteristicually absent from

wirbidite sand bodies. Medium seale foresets

(30-90 cm) of Staufler (1967) occur With

ripple marks of current and wave types. and

have been Interpreted as shallow water tric

how sediments rather than mass How deposits.

Foresets to 1 m high in the Dimple Limestones

(Texas) have been interpreted ay part of a

proximal turbidite facies with deposition under

‘high energy" conditions on the outer shelf

or upper slope (Thomson & Thomasson 1969),

Large scale low angle cross-bedding has alse

been observed in interpreted proximal tur

tidites by Corbett (1972) and Link (1975),

while Stanley (1964) regarded them as re»

presenting deposition as submarine depression

fillings and as fan shaped accumulations at the

buse of steep palacoslopes.

Mute) (1977) has defined a channel mouth

facres for the Eocene Hecho Group in Spain,

which has marked similarities fo sequence 2

deposits, That is, the deposits oecur in a

thickening and coarsening wpward sequence,

individual beds lense, wedge and amalgamate

over short distances, latge seule cross laminae

are common, and internal depositional struc.

tures are indicative of mainly tractional pro-

cesses without substantial fallout. Mutti com-

ments on the dissimilarities to previously de-

scribed tucbidiles and other mass How deposits.

The proposed model of Mutti is for deposition

of excess sand from the turbidity current as

it leaves the confines of a channel and spreads

out as a sheet flow across the lower fan, Sand

dropped from the by-passmny turbidity current

forms a bed of loose sediment that is reworked

through dune and ripple phases by the same

or subsequent currents. Thus prograding sand

lohes develop al (he dehowching terminus of

channels, as ts interpreted for deposition near

middle fan channels of the San Salvatore Sand-

stone (Mutty 1974). The middle fan environ-

ment is kaown to have a hummocky topo-

graphy from surface echo sounding profiles

(Normark 1974) and fs interpreted to contain

small delta or fanlike deposits at the end of

leveed vallevs (Normvark 1970). The dune

phase of Mw (1977) has probably been ob-

served, Shepard et a/, (1969) noted large sand

Waves with wavelengths of 15-30 m and up to

1 m high in the outer fan valley of the La Jolla

fan valley, where the channel merges with the

flat Moor of ihe San Diego Trough. The effect

FAN SEDIMENTATION—KANMANTOO GROUP

of the transition from confined ta uncanfined

turbidity flows is probably the same as a

decrease. in slope of the depositional surface.

Sequence 2 deposits are interpreted to re-

presen! a prograding sand bulge or lobe from

deposmon at channel mouths, Alternatively,

they may represent channelised turbidites near

a significant change of slope, e.g. palaecoscarps

ar transition from canyon to fan system, From

the random position of foresets in sequence 2

units, reworking of the loose sediment into

duve phases ls likely to be from the current

which carried the sediment, rather than sub-

sequent currents, The most likely environment

for channel mouth sedimentation is on the

middle fan (suprafan) depositional lobe, which

his been interpreted as the area of most rapid

aggradation (Piper & Normark 1971; Nelson

& Kulm 1973),

Based on the present-day models for deep

seu fans, sequence 1 and 2 deposits appear to

represent Sedimentation on a channelled supra-

fun and a suprafan depositional lobe. The eam-

bined thickness is several kilometres which is

well within the size estimates of 0.3-12 km

for modern deep sea fans (Nelson & Kulm

1973; Nelson & Nilsen 1974; Reineck &

Singh 1973). Predominantly sand deposition

from abundant and pulsating currents suggests

4 close proximity ta the source area(s),

Ancient landmasses to the northwest, west und

southwest (Gawler Craton extensions ar Ant-

arctic Shield) are indicated by the palaeoslope

and palacocurrents,

Tectonic delta camiple xyes

Occurrences of modern and ancient deltaic

complexes with significant sand ucposition and

which lave many similurities to Kanmaiitoo

Group sediments are.

1, Eocene Coaledo Formation, Qrezan (Dott

1966):

2. Carboniferuus sequence of Mam Tor

Series to Kinderscout Grit, Northern Eag-

land (Walker 1966; Collinson 1969)-

3 Holocene fuviemnarineg phases of the

Rhéne Della Complex (Oumkens 1970).

4, Devonian Chemung lithalacies of the

Catskill Delta Complex. New York

(Friedman & Johnson 1966);

§ Upper Opdoviefin Oswego Sandstone and

Reedsville Shale. Central Appalachians

(Horowitz 1968);

A. Tertiary debris flow and shallaw-water

density flow deposits of the Mackenzic

Delta, Canady (Glaister & Hopkins 1974),

249

Of these, the greatest sinmlarity in sedimen-

tary structures and lithologies of the Kanman-

too Group is with the Eocene Coaledo Formia-

lion, The deltaic model for Kanmantoo Group

lithologics would be sequence 2 deposits re-

presenting a distributary channel environment

on a delta platform, with sequence 1 deposits

ag slumps off the delta margin. Such a rapid

transition (rom ¢ross-bedded sandstone facies

lo proximal turbidites has been interpreted for

the Matilija Sandstone (California) by Link

(1975), Density currents off the delta have

been interpreted for the late Cretaceous to

Paleocene Difunta Group of northern Mexico

(Galloway 1975) while deltas with an asso-

ciated submarine slope and fan system are

deseribed by Asquith (1970) and Gallaway &

Brown (1972) Although those deltaic deposits

ure sandy in paris, sandy lithologies are no

more than hundreds of metres thick and grade

into lithologies with readily recognisable tidal

and subgerial characteristics. In Flinders Chase

no structures were observed to indicate depo-

silin above the storm wave base,

Although sediments similar to. Kanmantoo

Group lithologies are known from. tectonic

delta complexes, it ig concluded that the depo-

sits of Flinders Chase represent accumulation

ona deep sea fan.

Stratigraphic correlation

Recognition of some Kanmantoo Group

sediments in Flinders Chase us probable deep

sea fan deposits necessitates re-assessment of

regional correlations and depositional environ-

ments of Kanmantoo Group sediments in other

areas, A knowledge of the probable sedi-

mentary environments and possible regional

marker horizons are necessary before regional

cerrelatians are undertaken, Correlation of for-

mations based on individual structures or gross

lithologies are not necexsarily meaningful.

Sedimentary environments represented by

Kunmantoo Group sedimentation previously

have not been evaluated fully. Spriggs & Cam-

pana (19531 compare sedimentation with “the

Alpine Flysch”, hut Daily & Milnes (1973)

emphasise the possitility of shallow water sedi-

mentation, A deep water origin is presumed by

Skinner (1958) for the Nairne Pyrite Forma-

tran.

On available infermation (Daily & Milnes

1971, 1973) the mast likely correlative of West

Bay to Breakneck River sediments is the Tapa-

nappa Formation, which is equivalent to part

220

af the Inman Hill Formation of Thomson

(1969). Other possible equivalents are the

flackslairs Passage and Balquhidder Forma-

lions. However, this involves correlations over

100 km with litde intervening control, and

with deposition ij) 4 tectonically active environ-

Ment producing numerous local and regional

variations, Nevertheless, the similarity of Plin-

ders Chase sediments to these other forma-

lions sugeests a wider occurrence of deep sea

fan sediments within the Kanmantoo Group,

D, J. FLINT

Acknowledgments

This Work was supported and funded by the

South Australian Department ol Mines and

the Discipline of Marine Geology and Geo-

physics, Flinders University, The project

formed part of a B.Sc, (Hons.} thesis under

ihe supervision of Dr A. EB. Grady, Helptul

suggestions on an early draft of the manuscript

were made by Dr K, A. W, Crook and Dr V,

Gostin. The paper is published with permission

of the Director-General of Mines and Energy,

South Australia,

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A NEW GENUS ADELONEMA (NEMATODA: OXYURIDAE)

FROM AUSTRALIAN PHALANGERID MARSUPIALS

BY PATRICIA M. MAWSON

Summary

Adelonema n.g. is proposed for Oxyuris (s.l.) trichosuri syn. Syphacia trichosuri Johnston &

Mawson, hitherto known only from the female. Males are described from the type host Trichosurus

vulpecula and from T. caninus. The new genus is close to Austroxyuris J. & M. differing in the

development of structures in the buccal cavity, particularly clearly seen when examined by scanning

electron microscope.

A NEW GENUS ADELONEMA (NEMATODA: OXYURIDAE)

FROM AUSTRALIAN PHALANGERID MARSUPIALS

by Patricia M. MAwson*

Summary

Mawson, P. M. (1978) A new genus Adelonema (Nematoda: Oxyuridac) from Australian

phalangerid marsupials, Trans, RK. Soe, 8. Aust, 102(8), 223-226, 30 Novemher, 1978.

Adelonema 0g. is proposed for Oxyuris (s.1.) triehosur! sy. Syphacia trichosuri Johnston

& Mawson, hitherto known only from the female. Males ure described from the type host

Trichosurus vulpecula and from T, caninus. The new genus is close to dustroxyuriv J. & M.

differing in the development of structures in the buccal cavity, particularly clearly seen when

examined by scanning electron microscope.

Introduction

Female oxyurids were first recorded from

Trichosurus Vulpecula in Queensland as Syphe-

cia Irichosuri Johnston & Mawson (1938). The

description was revised later (Mawson 1964)

from fresh material in which only females

were present. Recently both males and females

have been taken from several host animals.

The species is found to differ from other

oxyunids so far described and a new genus is

proposed for it,

Adelonema gen. nov,

Diagnosis: Oxyuridae: Post oesophageal lateral

alae present. Head marked off from body hy

annular constriction and bearing four single

submedian papillae and two lateral amphids.

Mouth opening more or less circular, buccal

capsule more or less circular in transverse sec-

tion with six longitudinal ridges projecting

anteriorly as three large and three smaller

pseudolabia, Anterior end of oesophagus pro-

jects as three lobes into base of buccal cavity.

Ocsophagus long; excretory pore post ocso-

phageal. Mate: with ventral and lateral caudal

inflation, ending just behind cloaca, body end-

ing in long spike, Pour pairs of pedunculated

and one pair sessile caudal papillae. Spicule

single. Female: tail long, tapering; vulva about

mid body, uteri opposed; eggs not operculate.

Parasitic in Australian phalangerid marsupials,

Type species: Adelonema trichesuri (Johnston

& Mawson).

Discussion

Austroxyuris Johnston & Mawson, Parau-

stroxyuris Mawson and Macropaxyiris Maw-

son are distinguished from other oxyurids

(Petter & Quentin 1976) by the presence of a

buccal capsule with inter-radial lamellae, These

lamellae are present in the new genus, project-

ing as small lip-like cones. In addition Uiree

radial lamellae are developed at the anterior

end of the buccal capsule and project as three

cuticular lobes. These six projecting structures

are referred to as ‘pseudolabia’, as they appear

to arise from within the buccal capsule, not

from the cuticle around the mouth,

Adelonema trichosuri (Johnston & Mawson)

FIGS 1-6

Syphacia trichosuri Johnston & Mawson 1938, p,

194 (from Trichosurus vualpecule, Queensland).

Oxyuris (8...) trichesuri (Johnston & Mawson)>

Tiner (1948), p. 89; Mawson (1964), p, 259

from T. vulpecula, Queensland).

Hosts and localities; Trichosurus

Kerr, Kangaroo I, S. Aust; 7.

Ogilby, Clouds Creck, N-S.W,

Males 1,7-2.1 mm long, females 5.1-6.2

mim, Body of male almost cylindrical, ending

suddenly in tail spike, that of fermale tapering

very slightly to head and gradually in region

of tail. Lateral alae present in both sexes, from

base of oesophagus nearly to anal region.

Cuticle around mouth thickened, cushion-

like, with central circular mouth through which

Vulpecula

caninus

+ Department of Zoology, University of Adelaide, North Tce, S. Aust, 5000,

224 PATRICIA M. MAWSON

30 ym

Adelonema trichosuri. Fig. 1: Male. Fig. 2: Female. Fig. 3: head of female, lateral view. Fig. 4. pos-

terior end of male, ventral view.

ADELONEMA NEW GENUS (NEMATODA: OXYURIDAE) 225

Adelonema trichosuri. Fig. 5: anterior end of female. The three lips have lost their turgidity during

the drying process. Fig. 6: enlargement of part of Fig. 5, showing pores in cuticle, and part of

one (radial) pseudolabium.

project three prominent radial and three small

triangular inter-radial pseudolabia. Buccal cap-

sule more or less cylindrical thickened exter-

nally both anteriorly and posteriorly. Three

radial and three inter-radial ridges arise inter-

nally from buccal capsule at about its mid-

length, becoming larger anteriorly and project-

ing as six pseudolabia.

Oesophagus (345-375 ym in male, 850-

1100 »m in female), about 1/5-1/6 (male)

or 1/5-1/8 (female) of body length, with

nerve ring a little in front of its midlength.

Excretory pore post-oesophageal.

Male: ventral and lateral cuticle of posterior

end inflated, particularly just behind cloaca.

One pair of sessile and four pairs of pedun-

culate papillae of which third pair is very long.

Tail ends in spike 170-200 ,m long. Spicule

100-120 ym long, single, tapering, the distal

20 «wm less chitinised.

Female: Tail 960-1300 ym long. Vulva be-

tween 1/3-1/2 body length from anterior end.

Eggs 49-50 x 25-26 um, without operculum,

This species was considered by Mawson

(1964) to lack inter-radial plates in the buccal

capsule, but examination with scanning elec-

tron microscope showed that these are present

(Fig. 5). The same procedure showed the

presence of numerous fine pores over part of

the cuticle at the anterior end (Fig. 6). Speci-

mens from T. caninus are very slightly shorter

than those from Kangaroo Island.

Acknowledgments

I am grateful for the material from Tricho-

surus caninus which was kindly given to me by

Dr Paul Presidente, Veterinary School, Uni-

versity of Melbourne. The photo micrographs

were taken by E.T.E.C. Autoscan in the Cen-

tral Electron Optical Laboratory, University ot

Adelaide. I am indebted to Dr Karl Bartusek

of this laboratory for help in taking the photo-

graphs.