TRANSACTIONS OF THE

ROYAL SOCIETY OF SOUTH AUSTRALIA INC,

PARTS 1 &

Barker, S.

Mawson, P. M.

Plummer, P. S.

CONTENTS, VOL. 104, 1980

2, 29 FEBRUARY

New species and new synonyms of Stigmodera (Castiarina)

(Coleoptera: Buprestidae) - - - - - - -

Some strongyle nematodes (Amidostomum spp.) from Austra-

lian birds - - - - € - 4 - 2 P

Circular structures in a Late Precambrian sandstone: Fossil

medusoids or evidence of fluidization? - = - J -

Tyler, M. J. & Davies, M. Systematic status of Kankanophryne Hever & Liem

De Deckker, P-.

Viets, K. O.

PARTS 3 & 4,

Twidale, C. R.

Breed, W. G.

(Anura: Leptodactylidae) - - - - - 2

New records of Koonunga cursor Sayce, 1908 (Syncarida, Ana-

spidacea) - - - - e e m) nf = E

New Unionicolidae (Acari, Hydrachnellae) from Australia -

30 MAY

The Devil’s Marbles, central Australia - - = - -

Further observations on spermatozoal morphology and male

reproductive tract anatomy of Pseudomys and Notomys species

(Mammalia: Rodentia) - - - - - - -

Flint, R. B., Ambrose, G. J. & Campbell, K. 8. W. Fossiliferous Lower Devonian

Beveridge, I.

Mawson, P. M.

Ludbrook, N. H.

boulders in Cretaceous sediments of the Great Australian Basin

Progamotaenia Nybelin (Cestoda: Anoplocephalidae): new

species, redescriptions and new host records - 4 :

Beveridgea new genus (Nematoda: Strongylida) from the Agile

Wallaby from Northern Australia - - = - x 2

Non-marine molluscs from dolomitic limestones in the north

of South Australia - - - 4 f 7 \, ¥

NUMBERS 5 & 6, 28 NOVEMBER

Robinson, A. C. Notes on the mammals and reptiles of Pearson, Dorothee and

Greenly Islands, South Australia - - - - - -

Williams, D. L. G. Catalogue of Pisecahe wprtghtate fossils and sites in South

Australia - - 4 5 = :

Moore, P. S. Stratigraphy and depositional environments of the Billy Creek

Formation (Cambrian), east of the Flinders Ranges, South

Australia - - - - - - - - - -

Koste, W. & Shiel, R. J. New Rotifera from Australia = - - - - -

McNamara, K. J. Heteromorph ammonites from the Albian of South Australia -

Barton, C. E. & McElhinny, M. W. Ages and ashes in lake floor sediment cores

from Valley Lake, Mt Gambier, South Australia - ms -

von der Borch, C. C., Bada, J. L. & Schwebel, D. L. Amino acid racemization

dating of Late Quaternary strandline events of the coastal plain

sequence near Robe, southeastern South Australia - - ~

Glaessner, M. F. New Cretaceous and Tertiary crabs (Crustacea: Brachyura)

from Australia and New Zealand - - - - - -

van Beurden, E. & McDonald, K. R. A new species of Create Cerio

Hylidae) from northern Queensland - -

Jago, J. B. & Youngs, B. C. Early Papibetan tetas aoe the Olkie Basin,

South Australia - - 3 S

Fitzgerald, M. J. Muckera and Millbillillie—Australian achondritic meteorites -

101

167

171

193

197

201

Insert to Transactions of the Royal Society of South Australia, Vol. 104, Numbers 5 & 6, 28 November, 1980

NEW SPECIES AND A CATALOGUE OF STIGMODERA (CASTIARINA)

(COLEOPTERA: BUPRESTIDAE)

BY S. BARKER

Summary

Stigmodera rudis Carter is reinstated in the sub-genus Castiarina. Thirteen new synonyms are given

and two species are resurrected from the synonymy. One name has been wrongly synonymised. A

lectotype of S. rubriventris Blackburn is selected. Seven new species of Stigmodera (aliceae, aquila,

aurea, hateleyi, inflata, kiatae, mimica) are described and illustrated.

NEW SPECIES AND NEW SYNONYMS OF ST/IGMODERA (CASTIARINA)

(COLEOPTERA; BUPRESTIDAE)

by S. BARKER*

Summary

BARKER, S. (1980) New species and new synonynis of Stivmiodera (Castiarina) (Coleoptera,

Ruiprestidae). Trans. R. Soc. S. Aust. W4(1), 1-7, 29 February, 1980.

Stigmodera rudis Carter is reinstated in the sub-genus Costarina, Thirteen new syoonyms

are given and two species are resurrected from synonymy. One nume has been wrongly

synonymised. A lectotype of S. rbrivenriy Blackburn is selected, Seven new species of Stis-

madera (aliceae, aquila, aurea, hateleyi, inflate, hiatee, mintica) ave described and illustrated,

Introduction

Despite the wide occurrence of Stigmmdera

(Castiarina) species in Australia, some have a

restricted distribution, are not represented in

Museums and are difficult to obtain. Since my

catalogue of Stigmodera (Castiarina) (Barker

1979) 1 have borrowed or collected specimens

of a number of species previously unavailable.

From a comparison with types, photographs of

types and eXamination of male genitalia, | now

recognise seven new species and synonyms that

1 had missed previously.

Stigmodera (Castiarina) rudis Carter 1934

FIG. |

| have examined a complete male specimen,

It is a lycid mimic and, except that it has a

hairy head, antennae and pronotum, resembles

all other Stigniodera (Castiarina) and should

be included in the sub-genus. It was collected

on flowers of Leprospernum sp. at Lake Dob-

son National Park, Tasmania, at an elevation

of 914 m an 19.1.1951 by J, R. Cunningham,

Barker’s (1979) key to Stigmodera should he

modified so that the second phrase of the 2nd

couplet appertaining to Caytiarina Teads, “sel-

dom with hair on dorsal surfaces of head and

pronotum”.

Additions to synonymy of Stigniadera

(Castiarina)

australasiae L & G 1837, Mon, Bupr, 2, 32

assimiliy Hope (846, Trans. ent. Soc. Lond. 4,

212 (new synonym)

melbournensis Thomson 1879, Typ, Bupy, App,

la, 34

timida Kerremans 1898, Annals Soe, ent. Lely,

42, 147

* Department of Zoology, University of Adelaide,

Box 498, G.P.O., Adelaide, 8S, Aust. 500],

puerilis Kerremans 1898, Annis Soc, ent. Belg,

42. 147

varmined Saunders 1868, J. Linn, Soe. 9, 474

collivens Kerremans 1890, Bull. Soc, ent, Belg.

1890, 44 (new synonym)

felix Kerremans 1898, Anniy Soc, ent, Bela, 42,

142

dawsonensis Blackburn 1890. Trams. R. Soe. 8.

lust. 13, 155

pulchella Carter 1916, Trans, R. Soc, 8, Aust,

40, 135 (new synonyny)

deuqueti Carter 1927, Proc. Linn. Soe, N.S.W, 52,

225

sutton’ Carter 1932, Proc. Linn, Soc. N.S.W. 57,

104 (new synonym)

palazera Carter 1937, Trans, R, See, 8. Aust.

61, 125 (new synonym )

duaringae Carter 1929, Proc, Linn, Soe, N.S,

54. 6%

bagania Carter 1930, Proe, Lire

55, 534 (new synonym )

inermis Kerremans 1890, Bull. Soe. ent Belg,

1890. 45

nove Kerremans 1902, Getera Miser, 12, 208

rubella Carter 1931, Aust, Zool, 6, 345 (new

synonym)

media Hope (847. Trans. ent. Soe. Lond. 4, 284

seplemnoraa Carter W916, Tras, Re. Soe. §,

Aust. 40, 86 (new synonym)

yeplenemaculate Blackburn 1892, Trais, R. Soe.

S. dust. 1S, 45

piliventris Saunders (868, J. Linn, See, 9, 474

penerasa Kerremans 1898, Aanly Soc. ett. Bele.

42. [50 (new synonym)

rectifasciata Saunders 1868, J. Linn. Soc, 9, 472

vicilans Kerremans 1898, nals Soe. ent. Belg.

42, [43 (recognised by Blackburn 1900 p, 42)

riblounda Carter 1931, Aust. Zeel. 6, 346

Vielatra Denquet 1956, Proc. Linn, Soe. NSW.

81, 156 (new synonym)

rufipenniy USirby) 1818, Trans. Linn, Soe. 12, 456

crocipennis Le & G I837, Man. Bupr, 2, 21

crocipennix Hope 1846, Trans, enn Soe, Land,

1846, 292 Ma

qidadrijavedlard Obenberger 1933, Cay cal, Spel.

ent. 30, 69 (new synonyo)

Soe. NUS A.

2 S. BARKER

scalaris (Boisduval) 1835, Voyage de l’Astrolobe,

cyanicollis (Boisduval) 1835, Voyage de l’Astro-

lobe, 91

crucigera L & G 1837, Mon. Bupr. 2, 40

viridis L & G 1837, Mon. Bupr. 2, 46

crucigera Hope 1838, Col. Man. 2, 162

macleayi Blackburn 1892, Trans. R. Soc. S.

Aust. 15, 48 (new synonym)

prudens Kerremans 1898, Annls Soc. ent. Belg.

42,152

suavis Kerremans 1902, Genera Insect. 12, 210

crucioides Obenberger 1922, Arch. Naturgesch.

88, 118

Species resurrected from synonymy

I listed S. gravis Harold, 1869 as a synonym

of S. trifasciata L & G, 1837 (Barker 1979, p-

22). 8. gravis was a replacement name for S.

obscuripennis Saunders, 1868 which is a

homonym of S. (Themognatha) obscuripennis

Mannerheim, 1837. I have re-examined 10

Western Australian specimens in the South

Australian Museum collection. I find that they

are identical to a coloured photograph of the

type of S. gravis and I consider gravis a valid

species.

I also listed S. bucolica Kerremans, 1898 as

a synonym of S. trifasciata L & G, 1837. I

have re-examined 16 unidentified specimens in

the South Australian Museum collection, cap-

tured near Port Lincoln on the Eyre Peninsula,

S.A., and, on the basis of comparison with a

coloured photograph of the type, I consider

that they represent S. bucolica which I now

consider a valid species.

In the catalogue of Stigmodera (Castiarina)

I listed S. subnotata Carter, 1933 as a synonym

of S. subtincta Carter, 1933. It has been

pointed out to me that these are distinct, I

have examined material in the South Austra-

lian Museum and in the Western Australian

Museum and find that the male genitalia are

different; I consider both to be valid species.

In S. subtincta the last four visible abdominal

segments of males are testaceous and of

females metallic green. In S. subnotata all

visible abdominal segments are testaceous in

both sexes.

Selection of lectotype of S. rubriventris

Blackburn

Describing S. rubriventris Blackburn (1900)

p. 47 stated, “In one of the two specimens

before me.” The syntypes are males, one is in

the British Museum, the other in the South

Australian Museum. Most of Blackburn’s types

are lodged in the British Museum collection

and, all other things being equal, I consider

that the type should remain with the majority

of specimens. I hereby select the male speci-

men in the British Museum labelled ‘“W.A.

7556, S. rubriventris Blackburn” as the lecto-

type of the species.

».

»*

ney “ee

= b 4

aoe

5 mm

Fig. 1. Male Stigmodera (Castiarina) rudis Carter,

NEW STIGMODERA (COLEOPTERA: BUPRESTIDAE) 3

The abbreviations used in the text for

museum and private collections are as follows:

WADA, Western Australian Department of

Agriculture, South Perth; GB, Mr G. Burns,

Mornington, Vic.; ANIC, Australian National

Insect Collection, C.S.1.R.O., Canberra; JH,

Mrs J. I. Harslett, Amiens, Qld; AM, Austra-

lian Museum, Sydney; SAM, South Australian

Museum, Adelaide; WAM, Western Australian

Museum, Perth; MP, Mr M. Powell, Mr. M.

Golding & Mr T. M. S. Hanlon, Perth; NMV,

National Museum of Victoria, Melbourne.

Stigmodera (Castiarina) mimica sp. nov.

FIGS 2A, 3A

Types: Holotype: 3, Goldsborough near Gordon-

vale, Qid, 5.i1.1962, J. G. Brooks, SAM 121, 106.

Allotype: @, same data as holotype, SAM 121,

107. Paratype: | ¢, Marmor, Qld, xi.1946, W. du

Boulay, WAM.

Colour; Head, antennae black with blue reflec-

tions. Pronotum, scutellum black. Elytra red-

brown with black anterior margin, entire apex

black, curving upwards from margin 2/3 along

its length. Undersurface and legs black with

blue reflections. Hairs silver,

Fig. 2. (x3) natural size. A. Stigmodera mimica sp, nov.

inflata sp. nov.

aurea Sp. nov.

D. S. aquila sp. nov.

E. S. aliceae sp. nov.

Shape and sculpture: Head with small close

punctures, median groove between eyes,

muzzle short. Antennae: segments 1—4 ob-

conic, 5-11 toothed. Pronotum with small

close punctures; median basal fovea projecting

forwards as median impressed line to anterior

margin; glabrous basal notch on each side 1/3

from margin to centre; anterior to basal

notches a large irregular depression on each

side; anterior margin projecting forwards in

middle; basal margin bisinuate; laterally

rounded out from base, widest 1/3 from base,

rounded to apical margin. Scutellum: heart-

shaped; without punctures; convex in middle;

both lobes elongate. Elytra: three broad costae

on each side, scutellary, 3rd and 5th intervals;

other intervals punctate-striate and flat at basal

end, convex at apical end, punctured and

rough; laterally angled out from base, rounded

at shoulder, concave until after middle,

rounded to apex which is bispinose; spines very

small, rounded between; apices slightly diverg-

ing. Undersurface with small close punctures

and short close hairs. Last visible abdominal

segment truncate in both sexes. Male with

nn ®

B. S. hateleyi sp. nov. C.,

F. S. kiatae sp. nov. G.

4 S. BARKER

reduced tarsal pads on 2nd and 3rd legs,

pads absent on segments I-3 replaced with

single median spine, pad present on segment 4

only.

Size: Males 11.7 x 4.2 mm (2), Females 12,3

x 4.6 mm (1).

Distribution: North coastal Queensland.

General remarks; A lycid mimic belonging in

the §. sexplagiata group on the basis of male

genitalia and modified tarsal pads in male. An-

other member of the group S. erythroptera is

also a lycid mimic and has the same elytral

colour. S$. mimica differs from that species in

that it has fovea on the margins of the pro-

notum: S, erythroptera does not. S, mimica

has a different elytral pattern with more black

than in S. erythroptera. Elytral marking on §,

mimica is like that of S. nigriventris, also a

lycid mimic without costae on the elytra and

not a member of the S. sexplagiata group.

Stigmodera (Castiarina) hateleyi sp. nov.

FIGS 2B, 3B

Types: Holotype: &, Kiata, Vic., K. Hateley, SAM

121, 108. Allotype: 9, Kiata, Vic., K. Hateley,

SAM 121, 109. Paratypes: 5 3 & 2 9, same data

as holotype, SAM; 2¢' & 2 9, Wurarga, W. Aust.,

28.x.1978, M. Powell & M. Golding, MP, SAM;

1 2, Maranalgo Stn, W. Aust., 10.ix.1978, G.

Barron, MP; 1 9, Lake Grace, W. Aust., 16,x.1970,

K. & E. Carnaby, SAM; 2 ¢ & 1 9, Australia,

Blackburn & White, SAM.

Colour; Head, antennae, pronotum, most of

undersurface and legs dark blue with yellow

and green reflections, last visible abdominal

segment mainly brown in male. Scutellum

black. Elytra red-brown with following black

markings: narrow anterior margin; elongate

angled mark on each shoulder, rounded spot

between on suture all remnant of a pre-medial

fascia; post-medial fascia projecting forwards

in middle of each side and concave backwards,

not reaching margin; pre-apical mark extend-

ing over three intervals, concave forwards;

marks all connected down suture and covering

apex. Undersurface hairs silver.

Shape and sculpture: Head: closely and shal-

lowly punctured; median groove between eyes;

natrow ridge inside each antennal cavity;

muzzle short. Antennae: segments 1-3 ob-

conic, 4-11 toothed. Pronotum: shallowly

punctured; small median basal fovea extending

forwards to middle as glabrous line; basal

notch on either side closer to margin than to

middle; projecting forwards in middle of

apical margin; basal margin almost. straight;

laterally parallel-sided at base, rounded to

apex, widest 1/3 distance from base. Scutel-

lum: heart-shaped, with few punctures. Elytra

punctate-striate, intervals convex and pitted

with shallow punctures; laterally parallel-sided

at base, angled outwards, rounded at shoulder

then concave until after middle, rounded then

tapered to pre-apical area, then rounded to

apex which has no marginal spine, indented to

suture which has minute spines; apices not di-

verging, Undersurface shallowly punctured,

sparsely haired. Last visible abdominal seg-

ment truncate in males, rounded and narrowed

in females,

Size: Males 14.1 = 0.37 x 5.1 + 0.19 mm

(10). Females 14.6 + 0.36 x 5.6 = 0.13 mm

(8).

Distribution: Western Australia and Victoria.

General remarks; The elytral pattern and

colour are like those of §. rubriventris Black-

burn. However, S. hateleyi is a smaller spe-

cies, the male does not have a red abdomen

and male genitalia is different. Named after

Mr K. Hateley.

v" ¥

D E F G

Fig. 3. Photomicrographs of male genitalia of

Stigmodera (Castiarina) species: (A) mimica;

(B) hateleyi; (C) inflata; (D) aquila; (E) ali-

ceae; (F) kiatae; (G) aurea,

NEW STIGMODERA (COLEOPTERA: BUPRESTIDAE) 5

Sligmodera (Castiarina) inflata sp. nov,

FIGS 2C, 3C

Types Holotype: &, Baker's Creek Falls, Armi-

dale, N.S.W., 12.71,1979, T. J, Nuwkeswood, SAM

(21, 110, Allotype: 7, same data as holatype, SAM

T21, (iL. Purntypes: 6 4 & 13 9, Dungar Pally.

Armidale, NS.W.. 22/2401.1978, BS, & TO

Huwkeswood. SAM: 18 do & 3 2, same data as

holotype, SAM; 1 3 & 4 2, Dangar Falls, Arm

dale, NSW. 1O/145),1979, 7, J, Hawkeswood,

SAM,

Colours Head, antennae. scutellim, provotwm,

undersurface and legs bronze. Blytra yellow

with lollowing black markings: anterior tyar-

gin} pre-niedial faseia expanded at outside

ends into vittae Teaching basal and lateral thar-

Bins anteriorly and lateral margin posteriorly.

enclosing basal yellow spot on each side and a

spot on each shoulder, wide post-mechal fascia

reaching margin, concave in piddle of euch

side anteriorly and posteriorly: mark coverilig

whole apex: all marks connected down suture.

Hairs silver,

Shape and sculpture: Head: with close shal-

law puncnires; mediyn groove between eves;

muge shert. Antenme: segments J-4 ob.

conic, 5-t1 toothed. Pronotum closely pune

tured; shallow median basal fovea projecting

forwards to apex as median impressed line; an-

lerior margin slraight; basal murgin bisinviate;

Jaterally rounded froin huse, inflated io middle,

rounded to apex. Seutellum: shield-shaped;

concave in middle: with punctures, Elytra

punctate-striate, intervals convex more so ut

hase than apex; laterally angled out from base,

rounded at shoulder, convex until after the

middle then rountled und tapered to apex

which is bispinase; marginal spine larger than

sutural spine, rounded and indented between;

upices shehtly diverging. Undersurface with

shallow punctiires, covered in moderately long

hair) Last visible ahdominal segment sublrun-

ente in male. rounded in female. Tarsal pads

modified ow feet ef nrales: Ist leg, tarsal pads

absent on segments 1 & 2, reduced on 3; 2nd

Ter, tarsal pad absent on se#ment 1, reduced

on 2; 3rd leg, tarsal pad on segment 7 minute,

reduced an 2 & 4: on each foot central spine

present on undervurfaee of tursal segments |.

2 & 3 getting progressively smaller mm that

order.

Sizes Males 10.9 + 0.12 x 3.9 * 0,04 nim

(26). Females 117 > O17 x 4.4 = 0.0% mm

(211,

Distribulions New England district, N.S,W-

General remarks: Close to § wilsoni on simi

Jaritics in male genitalia, but Js Targer than that

species. The pronotum is More prominently in-

fated in the new species. In S. tei/soni the only

shoulder marking is « single vitea on each siile.

In 5. inflata the vittae are confluent with a pre

medial fascia, All specimens were collected on

the flowers of Bursaria spinosa,

Stigmodera (Castiarina) aquila sp. nov.

FIGS 2D, 3D

fypes; Holotype: ¢@, Gleneagle, W, Aust,

15,1971, K, 7. Richards, ANIC, Paratypes: 4 ¢,

same data as holotype, SAM & WADA.

Colour: Head, antennae, pronotum, scutellum,

undersurface and legs dull green, Elytra yel-

low wilh following black markings: anterior

margin; pre-medial fascia projecting Forwards

to lateral margin from anterior end only, post-

medial lascia reaching maryin, projecting for-

wards On each side from near margin; pre-

apical fascia not reaching margin; marks all

connected down sulure expanded at apex,

Undersurface hairs silver.

Shape und sculpture: Head: closely punctured;

median groove hetween eyes; muzzle sbort.

Antennae: segments 1-3 obconic, 4 4-toothed,

5-11 toothed. Protonum; with close punctures,

median basal fovea; projecting forwards in

muddle of apical margin; basal margin barely

bisinuate: laterally parallel-sided at ase.

rounded at apex, widest before the middle. Seve

tellumm: heart-shaped; with punctures. Elytry:

punctate-striate, intervals slightly wrinkled,

convex at apex; laterally angled out from base.

rounded at shoulder, faintly concave until

after middle then rounded to apex which is bi-

spinose; marginal spine larger than sutural,

wounded and indented between, apices slightly

diverging, Undersurface with close, shallow

punctures; moderately hgiry; hairs lone. Last

visible ubdominal segment truncate in male.

Size: Males 11,0 © 0,34 ¥ 3.9 = 6.19 mm (5).

Distribution; Darling Ratees. Western Austra-

lia.

General remarks: Male genitalia of this species

show similarities to those of 8. xcularis, How-

ever, S. scalariy has alternate intervals on the

elytra slightly raised and the anterior margin

af the pronotum is straight. Also the pre-

medial Fascia is tepresented by two spots on

the shoulder. S, sealaris ts found only io

eastern Australia and nelther species ts repre-

seuted in South Australia. All specimelis were

collected on 4 svertea sp.

6 S. BARKER

Stigmodera (Castiarina) aliceae sp. nov.

FIGS 2E, 3E

Types: Holotype: 3, Montacute, Mt Lofty Rgs, S.

Aust., 3.xi.1963, S. Barker, SAM 121, 129. Allo-

type: °, same data as holotype, SAM 121, 130.

Paratypes: 2 d, Murray Bridge, Lea, SAM; 1

Mt Lofty Regs, 4.xii.1964, N. McFarland, SAM; 5

3 & 5 92, same data as holotype, SAM; 21 3 & § 9,

Athelstone, S. Aust., 22.x.1966, McFarland &

Newberry, SAM; 1 3, Horsnell’s Gully, 12.xi.1967,

S, Barker, SAM; 2 3 & 2 9, Para Wirra N.P., S.

Aust., 7.xi.1971, S. Barker, SAM; 3 ¢ & 1 @,

Uraidla, S. Aust., 23/28.xii.1974, A. Wells, SAM;

1 ¢, Sommerton, S, Aust., SAM; 1 3%, S. Aust.,

SAM,

Colour: Head, antennae, scutellum, undersur-

face and legs blue. Elytra yellow with follow-

ing black markings with purple reflections:

basal margin; pre-medial fascia expanded at

outside ends into vittae reaching basal and

lateral margins anteriorly and lateral margin

posteriorly, enclosing basal yellow spot on

each side and one on each shoulder; wide post-

medial fascia reaching margin; mark covering

whole apex; all marks connected down suture.

Hairs silver.

Shape and sculpture: Head: closely punctured;

median groove between eyes; muzzle short,

Antennae: segments 1-4 obconic, 5-11

toothed. Pronotum: closely punctured; median

basal fovea extending forwards as thin glab-

rous line almost to apex; basal notches on each

side closer to margin than centre; projecting

forwards in middle of apical margin, basal

margin bisinuate; laterally parallel-sided at

base then rounded to apex, widest before

middle. Scutellum: heart-shaped; with punc-

tures, Elytra: punctate-striate, intervals con-

vex, more so at apex than base; laterally

angled outwards from base, rounded at

shoulder, concave until after middle, rounded

to apex which is bispinose; both spines small,

rounded and indented between; apices diverg-

ing slightly. Undersurface shallowly punc-

tured; sparse very short hair, Last visible abdo-

minal segment subtruncate in male, rounded in

female. Tarsal pads modified on feet of male:

tarsal pads absent on segments 1 & 2 on all

feet, single central spine on undersurface of

segments 1-3 on all feet in descending size

from 1-3,

Size: Males 8.3 = 0.1 x 2,9 + 0,04 mm (38).

Females 8.5 = 0.22 x 3.0 + 0.08 mm (14).

Distribution: South Australia.

General remarks: Close to S. cruentata (Kirby)

on similarities in male genitalia. The two spe-

cies differ im the pattern of reduction of tarsal

pads in males. Named after Mrs A. Wells.

Stigmodera (Castiarina) kiatae sp. nov.

FIGS 2F, 3F

Types: Holotype: 3, Kiata, Vic., xi.1967, K. Hate-

ley, SAM 121, 131. Allotype: 9%, Kiata, Vic.,

xi.1967, K. Hateley, SAM 121, 132. Paratypes: 3

3d, Big Desert, Vic., 17/19.xi.1977, G. Burns, GB:

2 3 & 2 9, same data as holotype, SAM: 1 ¢ & 1

Q, Big Desert, Vic., 4.xi.1976, G. Burns, NMV &

GB.

Colour: Head, pronotum, scutellum, undersur-

face and legs purple-bronze. Elytra yellow

with following dark blue markings: anterior

margin; vitta from outer edge of anterior mar-

gin running to lateral margin, enclosing elon-

gate yellow mark on shoulder; rounded mark

on suture remnant of pre-apical fascia; post-

medial fascia expanded on suture and middle

of each elytron not reaching lateral margin;

apical mark covering whole apex, all marks

connected along suture. Hairs silver.

Shape and sculpture: Head: closely punctured;

median groove between eyes; muzzle short.

Antennae: segments 1-3 obconic, 4-11

toothed. Pronotum closely punctured; small

median basal fovea; anterior margin straight;

basal margin barely bisinuate; laterally

rounded from. base, widest }-distance to apex,

slightly tapered to apex. Scutellum: heart-

shaped; without punctures. Elytra punctate-

striate, intervals flat at apex, more rounded at

base; laterally slightly angled out from base,

rounded at shoulder then concave until after

middle, rounded and tapered to apex which is

bispinose; apical spine large, sutural spine

small, rounded and indented between; apices

slightly diverging; sub-serrate lateral margin

from post-medial region to apex. Undersur-

face with close shallow punctures, larger on

pre-sternal sclerites than on abdomen; hairy,

hairs moderately long. Last visible abdominal

segment truncate in both sexes,

Size: Males 9,2 = 0.20 x 3.3 + 0.07 mm (7).

Females 10.0 = 0.21 x 3.6 = 0.07 mm (4).

Distribution: Big and Little Desert areas, Vic-

toria.

General remarks: This species is distinct from

any other on the basis of male genitalia.

Stigmodera (Castiarina) aurea sp. nov.

FIGS 2G, 3G

Types: Holotype: ¢, 18 km E. of Maryborough,

Qld, on Leptospermum sp., 5.xi.1975, S. Barker,

SAM 121, 133. Allotype: 9, same data as holo-

NEW STIGMODERA (COLEOPTERA: BUPRESTTDAE) 7

type, SAM 121, 134, Paratypes: 1 9, same data as

holotype, SAM; 4 2, Maryborough, Qld, xi,1946,

E. Smith, NMV:; L & . Maryborough, 12.xii,

MIM, ANTC; | & Indooroopilly, 11 xi.1933,

ANIC; 2 ¢. Wide Bay, Qld, AM: 1 ¢, Rockhamp-

ton, Qld, 10,1,1946, JH; 2d & 3 2, Qld, du Boulay,

WAM.

Colour, Head, antennae, pronotum, scutellum

black with olive-green reflections, Undersur-

face and legs olive green, Elytra yellow at

basal end, apical end bright orange, with the

following black markings: basal margin; short

vitta on each shoulder reaching lateral and

basal margins; basal elongate rounded mark on

sulure; post-medial fascia expanded on suture

and close lo murgin, reaching margin; pre-

apical fascia not reaching margin; mark cover

ing apices: all marks connected down suture,

the last two broadly, Hairs silver.

Shape and sculpture; Head with small shallow

punctures; median groove hetween eyes:

muzzle short. Antennac; segments 1-3 ob-

conic, 4-11 toothed. Pronotum with small

shallow punctures: basal fovea projecting For-

wards to middle as glabrous linc; basal notch

on each side closer to margin than to middle;

anterior margin projecting forwards in middle;

basal margin bisinuate; laterally rounded from

hase, gradually narrowing to apex, basal angles

turned upwards. Scutellum: heart-shaped,

sides folded inwards from centre; without

punctures, Elytra punctate-striate, the intervals

convex and smooth, the margin flattened; luter-

ally angled out from base, rounded at

shoulder, concave until afler middle, rounded

and narrowed to apex which is bispinose; mar-

ginal spine large, sutural spine very small,

deeply indented between, Undersurface with

close shallow punctures: moderately hairy,

hairs medium Jength. Last vistble abdominal

segment, rounded and pushed in in middle in

both sexes. Males have modified tarsal! pads on

3rd leg. segments | & 2 have reduced pads,

spines not present,

Size: Males 8.9 + 0.9 x 3.2 ~ 0.03 mm (9),

Females 10.5 = 0.09 x 3.9 + 0.05 mm (9).

Distribution: South and central coastal Queens-

land.

General remarks: Close to 8, alternecostata on

the basis of similarities in male genitalia, How-

ever, §. aurea is a smaller species. the prono-

tum 1s continually narrowed from the base

whereas ii S, allernecosiata the pronotum 1s

widest before the middle. Sculpture and colour

pattern of the elylra also differ,

Acknowledgments

1 thank the following for their assistance:

Dr A. Neboiss, National Museum of Victoria;

Mr G. Holloway, Australian Museum; Dr

T. F. Houston, Western Australian Museumy

Mr K. T. Richards, Western Australign

Department of Agriculture; Dr M, W. R, de

V. Graham, Hope Department of Zoology

(Entomology), University of Oxford; Dr M,

Uhlig, Muscum of Natural Science, Hujnboldt

University, Berlin; Miss C. M, H. von Hayek,

British Museum (Natural History); Mr E, EF.

Adams, Edungalba: Mr G. Burns, Morning-

ton; Mr and Mrs K, Carnaby, Wilga; Mrs J,

Harslett, Amiens: Mr K. Hateley, Kiata; Mr

T.J, Hawkeswood, Nedlands; Mr J. Macqueen,

Toowoomba; Herr H, Mihle, Neusaess; Mr

M. Powell, Como; Miss H. Vanderwoude and

Mrs A, Wells, Department of Zoology, Uni-

versity of Adelaide, The Australian Biological

Resources Committee provided a grant-in-aid

of research

References

Barker. S. (1979) New species and a catalogtc

of Stigmodera (Castiarina) (Coleoptera, Bup-

restidae). Trans, R. Soe. 8, Aust. W3, 1-23,

Biackeurn, T, (1900) Further notes on Austra-

lian Coleoptera, with descriptions of new genera

and species, Ibid. 26, 35-68,

Carter, H. J, (1934) Australian and New Guinen

Soleoplera notes and new species No. IL Prec.

Linn. Soc. N.S.W. Sa, 252-269,

SOME STRONGYLE NEMATODES (AMIDOSTOMUM SPP.) FROM

AUSTRALIAN BIRDS

BY PATRICIA M. MAWSON

Summary

Amidostomum acutum is recorded from Anas superciliosa, A. platyrhynchos, Stictonetta naevosa,

Querquedula gibberifrons, Tadorna radjah and Himantopus leucocephalus, A. anseris from Cereopis

novaehollandiae; A. cygni from Cygnis atratus; A. biziurae from Biziaura lobata. Measurements of

most specimens examined and morphological notes on A. cygni and A. biziurae are given. A new

species, A. tribonyx, close to A. acutum, but distinguished by shorter spicules and very large

papillae, is described from Tribonyx ventralis.

SOME STRONGYLE NEMATODES (AMIDOSTOMUM SPY.) FROM

AUSTRALIAN BIRDS

by ParriciA M. Mawson*

Summary

Mawson, P. M.

(1980) Some strongyle nematodes (Amidostomum spp) from Australian

birds. Troms. Ro Soe. 8. duet, WC), 9-42, 29 February, 1980.

Amidastomum acutin is recorded from Anas superciliosa, A. platyrhynchos, Stictonetta

natvasa. Querquedula gibberifrons, Tadarna radjah and Himartopus leucocephalus, A. anseris

from Cereopsis novaehollandiaes A. eyeni from Cypnuy atratis; A. bizlurae from Bizlura

lehuia, Mensurements of most specimens examined and morphological notes on A. eveni and

A. biziurae are wiven, A new species, A. tribonyx, clase to A. acutium, bot distingwished by

shorter spicvles and very large cervical papillae, is described from Tribenyx veniralis,

(nirodection

Neniatedes of the genus Amidostomum

appear to be restricted to waterfowl; almost all

records are from anseriform and ralliform

birds, and a few fram eharadriform birds, ‘Lhe

genus was studied in some detail by Czaplinskt

(1962), Gf the 16 species then recorded, he

synonymised Ll, Pour species have been de-

scribed subsequently,

In the present work three of the species

recognised fy Czaplinski are identified from

Australian birds, one species he considered a

synonym is resurrected and a new species is

described.

Measurements of specimens examined are

tabulated, but those indicating the position of

herve ring, cervical papillae and excretory

pore are omitted in some cases. These

struciures, cspevially the first two, are par-

ticularly obscure in some species. The new

species is noleworlhy because of the unusually

large cervieal papillae.

Types of the new species will be deposited

in the South Australian Museum, and all other

material belongs to the Australian Helmintho-

logical Collection at present in the South Aus-

tralian Museum,

Awidostomum acutum (ftundaht)

Strangylus acutuy Laundahl, 1848.

Hosts und localilies; Anay supereiliosus Gmelin:

Hamley Bridge S.A. (2 cf), Westbury, Tas. (24 3,

(8 2): 4, plaryrhyuehas, Plinders t, Vas, 1 2, t

Qo; Srlerenena naevosa (Gould), Bool Lagoon,

S.A. (2 Bs Querquedulu gibberifrans S. Miiller,

Naracoorte, SA, (1 of); Querquedula sp., Ade-

laide, SA. 01 Sd: Tadorne radjalt Garnot, Humpry

Doon, NT, (1 @); Mimantopus [eucocephalus

Gould, Petermann Ra,, N_T, (1 &, 2 2),

* Department of Zoology, University of Adelaide,

Box 498, G.P.O., Adelaide, 8. Aust. 5001,

In his work on Antidoyromum, Czraplinski

(1962) gives a good account of A, aeurtin,

and referred a number of species fo is syno-

nymy. Except for A. dizivrae Johnston &

Mawson, this synonymy has been adopted

here, Reasons for this exception are given in

the account of 4, biziurae.

Measurements of specimens from <Anay

superciliaxus, which are most numerous and jo

good condition, are given in Table 1.

Amidostomum anseris (Zeder)

FIG. 2

Strongylus anseris Zeder, 1800.

Host and locality: Cereapsis novaehollandiae

Latham, trom Flinders £., Tas. (5 d, 7 9).

These specimens agree generally with the

description, figures and measurements given by

Czaplinski in his Summary of the species. The

only (and slight) difference is that the anterior

lip of the vulva, and in two specimens both

anterior and posterior lips, are enlarged (Fig.

2), Czaplinski describes this region as “vulva

provided with conspicuous hemispherical

bulge”, Measurements of these specimens are

given in Table 1,

Amidostomum biziurae Johnston & Mawson

FIG, |

Amidostomum biziurae Tohnston & Mawson, 1947.

Host and localities: Biziura labata (Shaw) from

Goolwa, S.A. (3 cd, 2 9), Barren Box Swamp,

N.S.W. (5 3, 5 2).

This species, originally described from one

female, was cedescribed from new material of

both sexes (Mawson 1959), The specimens

recorded here from the type host species and

new localities agree with this description.

Czaplinski (1962) placed 4. bizinrae in the

synonymy of A, aeutunr, apparently not having

seen this redeseription, However, he dis-

counted the prajeclions around the mouth,

10 PATRICIA M. MAWSON

TABLE 1. Measurements of Amidostomum spp. recorded here (um unless otherwise stated).

Species A, acutum A. cygni A, anseris A. tribonyx

Anas Himantopus Cygnus Cereopsis Tribonyx

Host superciliosus leucocephalus atrata novaehollandiae ventralis

Male (number) (5) (1) (2) (4) (3)

Length (mm) 9,2-11.4 7.2 15-17 12,3-15.5 7.6-9.7

Oesophagus 640-760 1280-1500 1450 650-856

rods occupy 90-95% 99% 81-84%

A—nr 250-300 350-400 260-280 240-250

—cp 360-410 520-600 350-400 280-350

—exp 300-420 520-600 320-340 -

spicules 130-140 140 190-200 280-312 100-110

gubernaculum 60-70 80 105-110 110-115 30

bucc. caps: length 9 8 12-13 15-16 10

ext. diameter 11-12 13 35 31-35 18-19

Female (number ) (5) ( (2) (4) (3)

Length (mm) 13.5—17.0 13.6-13.7 22.0-22.1 19.5-21.0 7.6-10.0

Oesophagus 760-850 1250-1550 1420-1650 650-730

rods occupy 96% 99% 84-86%

A—nr 250-300 350-390 350-390 210-240

—cp 300-400 500-550 500-550 300-310

—exp 300-490 500-505 505-550 _

bucc. caps: length 10-11 15-16 15-16 10-12

ext. diameter 12-16 17-18 36-40 36-41 18-22

tail 250-280 250-260 250-260 240-330 220-300

vulva—posterior end (mm) 2.4-2.8 2.7-2.8 3.8-3.9 2.7-3.1 1,8-2.5

eggs—L 80-90 91-95 89-90 90-95 90-95

—Br 50-51 42-45 50-51 45-55 50-52

regarded by the authors as one of the main

specific characters, as being enlarged labial

papillae. In fact these are not labial papillae,

but cuticular structures, containing no nerve or

other hypodermal tissue. The four labial papil-

lae and two amphids are seen behind the pro-

jections (Mawson 1959, figs 4-5). The projec-

tions are obvious on all specimens, and arise

in association with the anterior edge of the

buccal capsule.

The other striking feature of the species is

the embossed cuticular annules, which appear

on all specimens, and have not been seen in

any other species. A more detailed figure is

given of the spicules.

Amidostomum cygni Wehr

FIGS 3-5

Amidostomum cygni Wehr, 1933.

Host and locality: Cygnus atratus Latham, Ade-

laide, S.A. (13 3, 16 9).

This species was recorded from C. atratus

(syn. Chenopis atrata) from Tailem Bend,

S.A. by Johnston & Mawson (1947), but that

material did not include the posterior end of a

male. The present material is more plentiful

and a closer study has been made.

The measurements (Table 1) are generally

larger than those given by Wehr (1933) or by

Ryzhikov (1959). Czaplinski (1962) regards

A. similis Freitas & Mendonca (1954) from a

South American swan a synonym of A. cygni:

the only difference being in the greater size and

in that. the authors noted three instead of two

(Ryzhikov) branches to each spicule, Wehr

simply states that the spicule is “similar in

shape to those of other species of the genus”.

In the Australian specimens there are three

branches, one much shorter and thinner, the

other two lying close together except at the

tips where one ends bluntly, the other is

splayed out. In the expanded state all branches

support a membranous structure which appears

to be globular rather than fan-shaped (Fig. 4).

Amidostomum tribonyx sp. nov.

FIGS 6-10

Host and localities: Tribonyx ventralis Gould,

from Swan Reach (3 3, 3 9), and Taperoo (1 6,

19), S.A.

Holotype male, SAM, V1864. Allotype female,

SAM, V1865.

Lateral alae absent, buccal capsule stoutly

built, with single, dorsal tooth reaching almost

to anterior edge of buccal capsule, Oesophagus

widens slightly posteriorly. Cervical papillae

prominent cuticular projections.

Male: Spicules bifid, each branch alate,

rounded at distal end, the more ventral branch

AUSTRALIAN NEMATODES (AMIDOSTOMUM) 1]

100 pm

Fig. 1. Amidostomum hiziurae, spicule.

Fig. 2. A. anseris, vulvar region.

Figs 3-5. A. cygni. Fig. 3, anterior end; Fig. 4, posterior end showing spicules partly everted; Fig.

5, posterior end of female.

Figs 6-10. A. tribonyx. Fig. 6, anterior end; Fig. 7, head; Fig. 8, bursa, ventral view; Fig. 9, dorsal

ray; Fig. 10, posterior end of female.

Figs. 1, 8 & 9 to same scale; Figs 3 & 5 to same scale: Figs 4 & 10 to same scale.

12 PATRICIA M. MAWSON

slightly longer. Gubernaculum poorly sclero-

tized, about + length of spicules. Bursal rays

typical of genus( Figs 8 & 9).

Female: Tail widens about midlength, at level

of phasmids, then narrows to rounded tip.

Vulva at about + body length from posterior

end, with swollen anterior lip.

This species differs from A. acutum in the

smaller spicules and gubernaculum, and from

all congeners by the large cervical papillae.

Measurements are included in Table 1.

Acknowledgments

The birds from which the material used in

this work were obtained were sent to me by Mr

H. Frith (C.S.I.R.O., Canberra), the Northern

Territory Museum, the South Australian

Museum, and Mr R. Green (Victoria Museum,

Tasmania).

References

CZAPLINSKI, B. (1962) Nematodes and acantho-

cephalans of wild and domestic Anseriformes

in Poland. 1. Revision of the genus Amido-

stomum Railliet & Henri, 1909. Acta Parasit.

Polonica 10, 125-164.

Freitas, J. F. T. & Menponca, M. J. (1954)

Novo tricostrongylideo parasito de cisne europen

(Nemaetoda: Strongyloidea). Rev. Brasil. Biol.

14, 397-400.

Jounston, T. H. & Mawson, P. M. (1947) Some

avian and fish nematodes, chiefly from Tailem

Bend, South Australia. Rec. S. Aust. Mus. 8,

547-553.

LUNDAHL, C. (1848) Helminthologische Beitrage.

1. Bemerkungen iiber zwei neue Strongylus

Arten. Notis. sdllsk. Fauna Flora Fenn. Forh. 1,

283-287.

Mawson, P. M. (1959) Some nematode parasites

from Australian hosts. Trans. R. Soc. S. Aust.

82, 151-162.

Ryzuikov, K. M. (1959) Nematodes in the heart

of a swan. [In Russian] Priroda 48, 119.

Wenr, E. E. (1933) Description of two new

parasitic nematodes from birds. J. Wash. Acad.

Sci. 23, 391-396.

ZeDER, J. G. H. (1800) Erster Nachtrag zur

Naturgesichte der Eingeweidewiirmer mit Zu-

faissen und Anmerkungen herausgegeben. 320

pp. Leipzig.

CIRCULAR STRUCTURES IN A LATE PRECAMBRIAN SANDSTONE:

FOSSIL MEDUSOIDS OR EVIDENCE OF FLUIDIZATION?

BY P. §S. PLUMMER

Summary

Small circular structures have been found preserved on the basal surface of a Late Precambrian

sandstone within the Moorillah Formation in the Flinders Ranges, South Australia. Although their

mode of preservation and general appearance suggest a biogenic origin, it is believed that a non-

biogenic process involving gas migration and sediment fluidization was responsible for their

formation.

CIRCULAR STRUCTURES IN A LATE PRECAMBRIAN SANDSTONE:

FOSSIL MEDUSOIDS OR EVIDENCE OF FLUIDIZATION?

by PS. PLUMMER*

Summary

Promune, PS. (1980) Circular structures la a Late Precambrian sandstone: Fossil medusoids

ov evidenve of Mhudization Trans, R. Soc. §. Aust. 104 (1), 13-16, 29 February, 1980.

Small cirenla: structures have been found preserved on the basal surface of a Lale

Precambrian sandstone within the Moorilah Formation in the Flinders Runges, South Australia.

Although their mode of preservation and general appearance suggest o biogenic origin, it is

believed that 8 non-hiogenic protess involving gas migration and sediment fluidization was

responsible for their formation.

Introduction

Recently found within the central Flinders

Ranges of South Australia was a float sample!

of ripple cross-luminated fine sandstone on the

basal surface of which are preserved a number

ot small, roughly circular structures of prob-

lematic origin. The sample was collected about

10 knv southeast of Wilpena Chalet (lat.

31°36'S, long, 138°40°E) near the contact be-

tween the Moorillah Formation and the under.

lying Moolooloa Formation of the Late Pre-

cambrian Brachina Subgroup (Plummer 1978),

Tts lithology is typical of the lower portion of

the Moorillah Formation and, although the

sample 15 from floal, it is considered to have

come fram this horizon,

A passible biogenic origin for these struc-

tures is suggested if their mode of preservation

(i.e, on the basal surface of a sandstone lying

directly above w clay layer) is compared with

that of the many soft-bodied animal fossils

fond within the Late Precambrian Ediacara

assemblage (sce Wade 1968). This, along with

their overall cireular shape and concentric

rings tarking their perimeters, suggests a

resemblance to small medusoid fossils. If this

were so, they would form perhaps the oldest

fossil coelenterale oecurrence known, lying

2500 m helow the level of the Ediacara assem-

blaee. and well beneath the presently knows

oldest occurrence in the Bonney Sandstone

(formerly the “Red Pound") of the Pound

Suheroup where small medusoids ure found in

association with sinuous tracks (Wade 1970).

*Centre for Precantbriun Research, Department

af Geology, University of Adelaide, Adelaide,

GPO, Box 498, 8. Aust, SOOT,

1 Sample in Department of Geology, University of

Adelaide: cat, No, 469/RPB1 LO.

Description

The basal surface of the sample measures

16x 171 em and shows several roughly circular

structures which range 6-20 mm in diameter

with relief up to 2 mm (Pig, 1a). The centres

of these structures are generally shallowly

domed (Fig. lb), although some ate Slat, or

display a central depression (Fig. 1¢). Poorly

ilefined step-like concentric rings are present

toward the edges of some of the structures

(sce Fig. 1b), whilst surrounding them is the

suggestion of a Mat skirting rim up ta 8 mm

wide, Shaly material is patchily preserved om

this basal surface of the sample, indicating that

the ripple cross-laminated sand formed casts

of these structures which were developed in,

or present on an underlying clay bed.

Interpretation

These structures are comparable to the fossil

medusoids classed as Prefelvella Torell 1870,

which includes the taxon Medtsina Sprivg

1949. Protolyella 3s represented by circular

bodies up to 5 cm diameter, comprising a

smooth central area and an outer annular

yone, separated by an annular furrow (Moore

1956; Glaessner & Wade 1966). Although the

central area of these fossils can show faint con-

centric markings, the outer annular zone

usually displays numerous radial grooves not

present on the structures described herein.

Other widely distributed circular organic

structures of Late Precambrian age ate the

planktonic remains known as Chnaria Walcott

L899, These fossils, however, are usually pre-

served as black, discoidul compressions, com-

manly carbonaceous, and having a maximum

diameter of 5 mm (Hofman 1977). As such,

the structures described here are too large and

of the wrong style of preservation ta be

Chuaria.

14 P. S. PLUMMER

Fig. 1. Circular structures. (a) casts on basal sur-

face of sample; (b) shallowly domed centre;

Maxson (1940) and Cloud (1960) have in-

terpreted structures comparable to those under

discussion in terms of gas escape and fluidiza-

tion phenomena, Such phenomena are well

known to igneous geologists (e.g. Reynolds

1954; Holmes 1965), but their influence upon

sedimentation has been little discussed. Mills

(1969), however, gives an excellent account

of structures formed experimentally by ‘cold’

fluidization which closely resemble the struc-

tures discussed herein. Although his experi-

ments were concerned with the origin of

craters on the lunar surface, the phenomenon

of ‘cold’ fluidization is equally applicable to

much smaller scale structures.

The process of ‘cold’ fluidization involves

the migration to the surface of gas trapped

within a stationary bed. In a cohesive sedi-

ment, such as a clay, gas migration can cause

the bed to expand and display the flow proper-

ties of a liquid. Often the gas flow finds pre-

ferred channels of escape and, if the flow is

great enough, bubbles may form in the chan-

nels. On reaching the surface the bubbles

either burst, or dissipate gently (depending on

the degree of bed cohesion) causing the bed

to then contract and subside. Ring slumping

and faulting often accompanies the subsidence,

Burial by Capping | Sand

nvr wha

\ I

x ee ee

Gas Migration

Fig. 2. Schematic diagram of crater formation by

‘cold’ fluidization process.

and the net result is the production of circular,

crater-like structures.

Such a process could have operated to pro-

duce the structures found on the sample de-

scribed here. Sedimentologic analysis has indi-

cated that the Moorillah Formation was depo-

sited dominantly within an intertidal environ-

ment (Plummer 1978). During a period of low

tide, gas or air trapped within sandy sediment

could have migrated upward through a cap-

ping clay layer (possibly deposited during the

slack-water stage of the previous high tide) to

burst and form small craters on the surface.

Gas escape phenomena are known to occur on

present-day intertidal flats (Reineck & Singh

1975, Fig. 61), and the burial of such craters

by a layer of sand during the following incom-

ing tide could then preserve them as casts on

its basal surface (Fig. 2). Such gas produced

structures have been called ‘evasion marks’ by

Cloud (1960), who differentiated them from

‘contact marks’ produced by single, or

numerous gas bubbles blown across the sedi-

ment surface; raindrop impressions (Lyell

1851, Shrock 1948); and other ‘pit-and-

mound’ structures produced by compaction-

induced dewatering (Kindle 1916, Schofield &

Keen 1929), or current flow stress (Karez et

al. 1974).

Other organic structures?

Also reported from the Moorillah Forma-

tion are other structures which were initially

LATE PRECAMBRIAN CIRCULAR STRUCTURES 15

believed to be of organic origin, The solitary

trace-like murking BSanyerichnius dalgarnoi

Glacssner 1969 was deseribed as the track of

an animal possibly "related to primitive mol-

lusea without mineralized shells” (Glyessner

1969, p. 379). However, Jenkins (1975, p, 19)

regarded jl “a unigue and accidental set of

markings made by a tethered implement being

moved by a current’ (eg. possibly ribbon-like

algae such as are known from cocks of similar

age in the U.S.S.R.), A close resemblance is

also noted between this marking and certaln

lineations produced by vorticity along lines of

wind flow (Whitney 1978, Fig, 4B). Also.

abundant cylindrical to coni¢al structures

ecelir in this formation that resemble either

certain fossil burrows of other problematic

Precambrian sack-shaped fossil organisms such

us Namalia Germs 1968, the ‘Erniettomorpha’

of Pilg (1972) and Baikalina Sokolov 1972.

These structures, however, are pol-casts pro-

duced by the helical scouring action of water

currents (Jenkins ef al, ih prep.).

Conclusion

Of the two possible origins presented to

explain the structures discussed herein (viz.

the fossilization of small medusoids, or gas

escape and ‘cold’ fluidization phenomena) the

latter, non-biogenie origin is fuvourcd, Simi-

larly, olher circular structures found in depo-

sits of Precambrian age that have previously

been deseribed as problematica or organic

remains (e.g. Bassler 1941, Alf 1959, Shep-

heed & Thatcher 1959, Johnson & Fox 1968)

should be feViewed in lerms of formation by

fluidization phenomena, or other imorganic

processes (as suggested by Cloud 1940, 1973},

Acknowledgments

Dr R. J, F. Jenkins provided much discus-

sion on Precambrian life forms and traces,

whilst both he and Dr V. A, Gostin evitically

read the manuscript.

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Proterozoic Buss Formation, Grand Canyon,

Arizona. Plated 31, 60-63.

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preCambrian at the Grand Canyon. Proc. U.S.

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Croup, P. BE. Je, (1960) Gas as a sedimentary

and diagenetic agent. Aim. J. Nei 258A, 35-45.

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in the Nunia System, South-West Africa, Nutire

259, 53-54,

GLaessvNeR, M, Fb, (1969) Trace fossils from the

Precambrian aud basal Cambrian. Lethaia 2%,

369-393.

GLAgssNek, M. F. & Wank, M-. (1966) The Lute

Precambrian fossils from Edivears, South Aus-

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Hormawn, H, J. (1977) The problematic fossil

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Jenkins, Ro J F. (1975) The diversification of

early metazoans. Absir Ist Aust. geol. Conv.

weal. Soc. Attist, 19-20,

Jenkins. R$. F.. Plunmier, P. S. & Montarry,

K. C. fin prep.) A South Australian find of

abiindant Late Precambrian pseudofossils fe

thatkubly fesembling |rue fossils of comparable

age.

Jonwsomn, H. & Fox, 8. K.. Jr. (1968) Dipleurozea

from Lower Silurion of North America. Scievice

THz, (19-720,

Kancz, 1, Enos, P. & Lancinrr, G, (1974)

Stuctires generated in fluid stressing of freshly

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structures deVeloped during sedimentation. Geel,

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Recent, Triassic and Carboniferous periods.

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and possible implications fur the orwgin oF lunar

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Prummepr, PS, (1978) The stratigraphy of the

lower Wilpena Group (Late Precambrian),

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16 P. S. PLUMMER

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Soc. Am. 89, 1-18.

SYSTEMATIC STATUS OF KANKANOPHRYNE HEYER & LIEM (ANURA:

LEPTODACTYLIDAE)

BY M. J. TYLER & MARGARET DAVIES

Summary

The diagnostic characters of Kankanophryne Heyer & Liem (1976) that distinguish it from the

Pseudophryne Fitzinger (1843) were stated to be in the form of the sacral diapophyses and the

number of slips of the Musculus depressor mandibulae. Our survey of these features in the two

genera fails to support any distinction; hence we propose that Kankanophryne be referred to the

synonymy of Pseudophryne.

SYSTEMATIC STATUS OF KANKANOPHRYNE HEYER & LIEM

(ANURA: LEPTODACTYLIDAE)

by M. J. TyLer & MarGarer Davyies*

Summary

Ty.eR, M. J. & Davies, M. (1980) Systematic status of Kankanophryne Heyer & Liem

(Anura: Leptodactylidae). Trans, R. Soc. 8, Aust. 104(1), 17-20, 29 February, 1980,

The diagnostic characters of Kaukanophryne Heyer & Liem (1976) that distinguish it

from Pseudophryne Fitzinger (1843) were stated to be the form of the sacral diapophyses

and [he number of slips of the Musculus depressor mandibulae, Our survey of these features

in the two genera fails to support any distinction; hence we propose that Kankanophryne be

referred to the synonymy of Psevdophryne.

Introduction

Heyer & Liem (1976) undertook an analysis

of intergeneric relationships in Australian

myobatrachid (leptodactylid) frogs. Amongst

their consequent proposals was the erection of

the genus Kankanophryne for Pseudophryne

occidentalis Parker, described from Western

Australia (Parker 1940) and reported from

South Australia by Tyler (1972). The rationale

for Heyer & Liem’s action was the stated

existence in P. occidentalis of a small series of

character states not shared by congeners. The

authors stated that these were “differences best

reflected at the generic level” (1976, p, 5).

Tyler (1978) failed to adopt the new

generic name, but Cogger (1978) has included

Kankanophryne in the revised edition of his

“Reptiles and Amphibians of Australia”, Be-

cause Our observations on the definitive

characteristics involved are at variance with

those published by Heyer & Liem, we present

these data here to clarify the systematic status

of Katikanophryne.

Our retention of the name Leptodactylidae

instead of adopting Myobatrachidae reflects

the absence of morphological substantiation

for the latter step. This matter is discussed in

detail by Tyler (1979).

Material and Methods

We have examined the external features,

myology and osteology of representatives of

the following species: Pyeudophryne bibroni

Giinther, P. coriacea Keferstein, P. guentheri

Boulenger, P. occidentalis and P. semimar-

morata Lucas. Specimens are deposited in the

collections of the South Australian Museum

* Department of Zoology, University of Adeluide,

Box 498, G.P.O., Adelaide, S.A. S001.

(SAM), Western Australian Museum (WAM)

and Department of Zoology, University of

Adelaide (UAZ).

Fig, L, Augles of sacral diapophyses measured.

SDAR: anterior angle of right sacral diopo-

physis; SDER: gpredtest expansion of right

sacral diapophysis; SDPR: posterior angle of

right sacral diapophysis.

18 M. J. TYLER & MARGARET DAVIES

Muscles were examined with the aid of the

iodine/potassium iodide stain developed by

Bock & Shear (1972). Bones and cartilage

were examined employing either cleared and

Alizarin Red staining or the differential Aliza-

tin Red/Alcian Blue stain (Davis & Gore

1947; Dingerkus & Uhler 1977). The method

of measurement of sacral diapophyseal angles

follows Trueb (1977) and is demonstrated in

Fig. 1.

Generic diagnoses

Heyer & Liem’s diagnoses of Pseudophryne

Fitzinger and Kankanophryne are identical in

the condition of the following features:

separation of cervical cotyles, lack of Musculus

omohyoideus, lack of columella, texture of

belly skin, form of toes, presence of metatarsal

tubercle and mode of reproduction.

The diagnoses differ in the following

respects:

Vomerine bones. Present or absent in

Pseudophryne; absent in Kankanophryne.

Sacral diapophyses: Broad in Pseudophryne;

narrow in Kankanophryne.

Depressor mandibulae:

fascia absent in Pseudophryne;

Kankanophryne.

It follows that the critical characteristics for

the recognition of Kankanophryne are the

conditions of the sacral diapophyses and de-

pressor mandibulae.

Slip from dorsal

present in

Expansion of sacral diapophyses

The definition of character state 12 in

Heyer & Liem’s paper is as follows: State 0:

sacral diapophyses expanded; State 1: sacral

diapophyses rounded uniformly, in at least

some species. They then proceed to score

P, occidentalis as State 1 and the remaining

species of Pseudophryne as State 0. Generic

descriptions of Kankanophryne and Pseudo-

phryne refer to “narrow” and “broad” sacral

diapophyses respectively.

The maiority of anurans have moderately

expanded sacral diapophyses (designated

“dilated” by Trueb (1973) ). Amongst the

Ranidae, however, the sacral diapophyses are

narrow and usually directed posterolaterally

whereas at the other extreme of the spectrum

(in the Bufonidae), sacral diapophyses are

very broadly expanded. Lynch (1971) con-

sidered that any distinction between the

degree of dilation of the sacral diapophyses

exhibited by some of the Australopapuan

leptodactylid genera he examined, is a very

fine one and probably is not defensible.

Trueb’s (1977) investigation into the osteology

of a population of Hyla lanciformis (Cope)

indicated that a degree of uncertainty exists

about the reliability of vertebral characters.

Vertebral anomalies are common amongst

anurans, particularly in the form of bilateral

asymmetry, and presence of additional features

such as transverse processes on the coccyx in

some individuals (unpublished observations).

Trueb (1977) observed that a low coefficient of

variability in the shape and orientation of the

anterior edge of the sacral diapophyses

occurred in her study population, indicating

that some sacral features are reliable for

systematic purposes.

We have carried out Trueb’s measurements

on the species examined by us and the results

are shown in Table 1. The vertebral columns

TABLE 1. Measurements of sacral diapophyses (see

Fig. 1) in individuals of Pseudophryne and Kan-

kanophryne.

Sacral angle measurement in degrees

Species SDAL SDAR SDEL SDER SDPL SDPR

P. bibroni 83.5 75.0 41,0 49.5 55.5 55.5

P. coriacea 68.5 72.0 49.0 39.5 62.5 68.5

P. guentheri 82.5 85.5 50.0 39.0 47.5 55.5

P.semimarmorata 69.5 74.5 53.5 43.0 57.0 62.5

K. occidentalis 80.0 78.5 49.0 52.5 51.0 49.0

SDAL(R): Anterior angle of left (right) sacral dia-

pophysis;s SDEL(R): Greatest expansion of left

(right) sacral diapophysis; SDPL(R): Posterior

angle of left (right) sacral diapophysis.

of the species considered are shown in Fig. 2.

Whilst recognising that the measurements in

Table 1 have been made on individuals rather

than populations, it can be seen that there is

no significant difference in the expansion of

the sacral diapophyses between P. occidentalis

and the other species of Pseudophryne

examined by us, We can find no justification

for Heyer and Liem scoring the expansion of

the sacral diapophyses in P. occidentalis as

“narrow” in comparison with other Pseudo-

phryne.

Depressor mandibulae

Griffiths (1954, 1959) demonstrated the

existence of interspecific divergence in the

form of the M. depressor mandibulae, and the

way in which this divergence could be em-

ployed for systematic purposes. Griffiths

SYSTEMATIC STATUS OF KANKANOPHRYNE HEYER & LIEM 19

Fig, 2. Vertebral columns of (A) Pseudophryne semimarmorata UAZ B536, Koonwarra, Vic,; (B)

P, vecidestaliy, SAM R17522, approx. 100 km S of Balladonia Hotel, W.A. (33°13'S, 123°27'B);

garoo Is; (6) P. coriacea, UAZ BS37, Conondale Ra. Qld. Note similarity of shape of sacral dia-

popbyses and the numerous examples of vertebral bilateral asymmetry.

Fig, 3.

muscles. A: Pxevdophrvne semimarmorata; B;

Lateral view of Depressyor miundibulue

PL bibroni; C: PL veeidentilis, A slip of the

muscle occurs upon the dorsal fuscia in each

species. D.M main squamosal/otic element of

depressor mandibulae; O.M.p.fusc.; depressor

mandibulae pars fascialis; D.M.p.tyvmp,: depres-

sor mundibulue pars lympanicus.

recognised three conditions in the origin of this

muscle: (a) arising from the posterior border

of the otic arm of the squamosal, (b) arising

from the squamosal and the dorsal fascia and,

In some respects this descriptive system re-

presents. a simplification because the muscle

commonly comprises three elements: the third

arising from the tympanum and termed the

“pars tympanicus”.

Lynch (1971) examined the condition of the

depressor mandibulae in P. bibroni and P.

corroboree and reported that the genus has

only one slip — the pars tympanicus.

Our studies do not support the observations

of Lynch or those of Heyer & Liem. As illus-

trated in Fig. 3, each of the species examined

by us has Jarge squamosal and dorsal fascial

elements. The relative size of the dorsal fascia

element in P. occidentalis is mtermediate be-

tween that exhibited by P. bibroni and that in

the type species P. semimarmorata. In P,

guentheri the M. depressor mandibulae re-

sembles the condition in P. bibroné except that

the slip to the dorsal fascia is slightly smaller.

20 M. J. TYLER & MARGARET DAVIES

Discussion

Our observations indicate that the form of

the M, depressor mandibulae and sacral dia-

pophyses of P. occidentalis cannot be dis-

tinguished from the condition exhibited by the

type species of Pseudophryne (P. semimar-

morata). Kankanophryne was erected on the

premise that the species differed substantially

from Pseudophryne, but we are unable to sup-

port its maintenance, and we propose that

Kankanophryne be referred to the synonymy

of Pseudophryne.

Acknowledgments

This study was supported by a grant to

M.J.T. by the Australian Research Grants

Committee,

References

Bock. W. J. & SHEAR, C. R. (1953) A staining

method for gross dissection of vertebrate

muscles. Anat. Anz. 130, 222-7.

Coscer, H. G. (1978) “Reptiles and amphibians

of Australia”. 2nd Edtn (Reed, Sydney).

Davis, D. D. & Gore, U. R. (1947) Clearing and

staining skeletons of small vertebrates.

Fieldiana: Technique (4), 3-16.

Dincerkus,. G. & UHLER, L. D. (1977) Enzyme

clearing of alcian blue stained whole small

vertebrates for demonstration of cartilage.

Stain Technol, 52(4), 229-32.

GriFFITHS, J. (1954) On the “otic element” in

Amphibia, Salientia. Proc. zool. Soc. Lond.

124, 35-50.

(1959) The phylogeny of Sminthillus

limbatus and the status of the Brachycephalidae

(Amphibia, Salientia). /bid. 132, 457-87.

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

the intergeneric relationships of the Australian

frog family Myobatrachidae. Smithsonian

Contrib. Zool. (233), 1-29.

Lyncu, J. D. (1971) Evolutionary relationships,

osteology, and zoogeography of leptodactyloid

frogs. Misc. Publ. Univ. Kansas Mus. nat. Hist.

(53), 1-238.

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

the family Leptodactylidae. Novit. Zool. 42(1),

1-106.

Trues, L. (1973) Bones, frogs and evolution. Jn

J. L. Vial (Ed.) “Evolutionary Biology of

Anurans: Contemporary Research on Major

Problems”. (University of Missouri Press,

Columbia. )

(1977) Osteology and anuran systematics:

intrapopulational variation in Hyla lanciformis.

Syst. Zool. 26(2), 165-84.

TyLer, M. J. (1972) Discovery in the Everard

Ranges of a species of leptodactylid frog new

to the fauna of South Australia. Trans. R. Soc.

S. Aust. 95, 215-7.

— (1978) “Amphibians of South Australia”.

84 pp. (Govt Printer, Adelaide).

—— (1979) Herpetofaunal relationships of South

America with Australia. In W. E. Duellman

(Ed.) “The South American Herpetofauna: Its

origin, evolution and dispersal’, pp. 73-106.

Monogr. Mus. Nat. Hist. Univ. Kansas (7).

NEW RECORDS OF KOONUNGA CURSOR SAYCE, 1908 (SYNCARIDA,

ANASPIDACEA)

BY P. DE DECKKER

Summary

Koonunga cursor is recorded from two new localities, one in southwest Victoria and the other in

northwest Tasmania. Specimens are illustrated with scanning electron microphotographs and

drawings of the appendages.

NEW RECORDS OF KOONUNGA CURSOR SAYCE, 1908 (SYNCARIDA,

ANASPIDACEA)

by P. De DEcKKER*

Summary

Tie Deeckker, FP.

(1980) New records of Keonutga cirsor Sayce,

1908 (Syncarida,

Anuspidacea). Travis. Re Soe, 8, Aust, W4(2), 21-25, 29 February, Los.

Koonunga crrsar is recorded from two new localities, one in southwest Victoria and the

other in northwest Tasmania. Specimens aro illustrated with scanning electron microphoto-

graphs und drawings of the appendages,

Introduction

Most parts of South Australia are too arid

for anaspidaccan syncarid crustuceans to live—

permanent, natural freshwater bodies are rare

exeept in the southeast near Mi Gambier

where rainfall is highest, However, in Victoria

very close lo the S.A, border near Mt Gambier

the living syncarid Koonunga curser has

recently been found and is described here.

Diseussion

Sayee (1908) desvribed K. cursor from

“freshwater reedy pvols beside » ny funnel

joining the Mullum Mullum Creek at Ringwood

near Melbourne’. Drummond (1959) stated

that J, Searle in 1930 failed to find K, curser

in the type locality beeatise it had become a

storm-Wwater drain. However, in an introductory

account of crustaceans from Victoria, Morrison

(1955) mentioned that “Koonunga . ~~ had

been extensively collected by various members

of the Zoology Department of Melbourne

University . . .°. She also stated that “it now

appears that the Koonungidae are widely dis-

tributed, with local abundance, in an area

south of the Great Dividing Range extending

(rom Portland to Wilson's Promontory”. Un-

fortunately no localities were mentioned by

Morriso), Drummond's (1959) short note on

the Australian syneurids said that “Koonunga

lis}... now known to occur sporadically right

ucross the southern part of Victoria’. Never-

theless, he made no reference to particular

localities and none have since been reported,

Even Schminke’s (1978) paper, which tp-

cluded an Ulustration of the telson of a juvenile

specimen of K, eurser given him by FL H.

Drunymond, gave no locality data.

* Deparment of Zoology. Universily of Adelaide,

G.P.O. Box 498, Adelaide, S. Aust. 5001.

Recently K, curser has been collected from

the following localities, (1) Victoria, close to

the S.A. border, under the foothridge over the

rivulet at Bullocky Wells Picnic Area, 1.5 km

E of Greenwald on the main road between

Mt Gambier and Heywood (35°58'42"S,

141°23'09"B) 24, v, 1979; (2) northwestern

Tasmania, from Mowbray Swamp near Mella,

5 km W. of Smithton. This Tasmanian record

is the first to be published, although P. S. Lake

(in Williams in press) has informally reported

its occurrence there, No locality data were

given. At the Victorian locality, 15 females

and seven males were collected from floating

vegetution, The females were larger and

darker in colour than the males, Adult males

were easily recognized by the peculiar globular

organ attached to the antennule (Fig. 4, 9),

The largest female collected was 9.4 mm tong

(anterior tip of head to base of telson) and

ihe largest male, 5 mm long. In Tasmania,

several specimens were collected, but only one,

a female 7,8 mm long, could be examined after

Preservation,

An undissected female and male are

illustrated in Figs |-2, and particular featores

of their anatomy are shown in more detail in

Figs 3-8. To broaden Sayce’s (1908) deserip-

tion, the left appendages of one male specimen

from locality (1) were dissected (Figs 9-34).

These specimens are deposited in the Aus-

trallan Museum, Sydney, with two tindissected

specimens of each sex accompanied by the

Tasmanian specimen.

Acknowledgments

! thank Prof, W. D, Williams, Department

of Zoology, University of Adelaide, for en-

couragement. Dr K. F. Walker brought my

attenlon to the article by Morrison, Dr K.

Bartusek, P, Kempster and J, Wright (Uni-

versity of Adelaide) are thanked for help with

the SEM photography,

22 P. DE DECKKER

Figs 1-2. Koonunga cursor from locality (1). 1, undissected 9; 2, undissected ¢. Both at same mag-

nification. Scale: 500. Specimens frozen dried and coated with gold palladium before SEM photo-

graphy.

Figs 3-8. Koonunga cursor from locality (1). 3, detail of fig. 1 to show cephalon with transverse

sulcus; 4, detail of fig. 2 to show globular organ on ¢ antennule; 5, detail of fig. 2 to show ¢

copulatory appendages in ventral position; 6, detail of fig. 2 to show anterior appendages and globular

organs on antennules; 7, 9 telson viewed posterolaterally; 8, ¢ telson viewed ventrally.

Scale: 500 for figs 3, 6, 7, 8; 50 for fig. 4; 200” for fig. 5.

1S)

je)

wat

ON TH

ON THE SYNCARID KOONUNGA CURSOR 25

References

DRUMMOND, F. H. (1959) The syncarid crustacea, Sayce, O. A. (1908) On Koonunga cursor, a

a living link with remote geological ages. Aust. remarkable new type of malacostracous

Mus. Mag., 13, 63-4. crustacean. Trans. Linn. Soc. London, 11, 1-16.

ie Scuminke, H. K. (1978) Die phylogenetische

Morrison, P. C. (1955) Animal life. In ‘Intro- Stellung der Stygocarididae (Crustacea, Syn-

ducing Victoria’ (Ed. G. W. Leeper) pp. 69-81 carida)—unter besonderer Beriicksichtigung

(ANZAAS: Melbourne). morphologischer Ahnlichkeiten mit Larvenfor-

men der Eucarida. Z. zool. Syst. Evolut.-forsch.,

NicHoLts, G. B, (1931) Micraspides calmani, a 16, 225-39. ,

new syncaridan from the west coast of ‘Tas- Me tae a Bee? sane eee a

mania. J. Linn. Soc. London (Zool.) 37, ‘Biogeographical Ecology in Australia’. Junk,

473-88. The Hague,

Figs 9-34. Koonunga cursor & left appendages except for figs 24, 29. 9, antennule; 10, antenna; 11,

maxilliped; 12, first peraeopod; 13, endopodite p'ate of peraeopod; 14, second peraecopod; 15, man-

dibular coxale; 16, first maxilla; 17, third peraeopod; 18, second maxilla; 19, third peraeopod (claws

missing); 20, fourth peraeopod; 21, first pleopod with endopodite; 22, detail of tip of endopodite;

23, detail of tip of endopodite, different orientation; 24, right second pleopod with endopodite; 25,

detail of fig. 27—tip of endopodite of left second pleopod; 26, detail of fig. 27—-coupling spines; 27,

left second pleopod; 28, median appendage attached to sternum; 29, detail of fig. 24—tip of endo-

podite of right second pleopod; 30, detail of fig. 29—coupling spines; 31, fifth peraeopod; 32,

penultimate pleopod; 33, last pleopod; 34, third pleopod.

Note: not all peraeopod endopodites are illustrated. Top scale: 5004 for figs 9-21, 31-34; middle

scale: 3004 for figs 25, 28, 29; bottom scale: 100 for figs 22, 23, 26, 30.

NEW UNIONICOLIDAE (ACARI, HYDRACHNELLAE) FROM

AUSTRALIA

BY KURT O. VIETS

Summary

Seven new species of the water mite genus Unioncola, subgenus Pentatax (Acari, Hydrachnellae),

are described from Australian freshwater mussels: Unioncola (Pentatax) walkeri n.sp., U. (P.)

procursa n.sp., U. (P.) assimilis n.sp., U. (P.) conjunctella n.sp., U. (P.) ligulifera n.sp., U. (P.)

clipeata n.sp., and U. (P.) scutata n. sp. A further new species is placed in Unionicolopsis

opimipalpis n.g., n.sp.

NEW UNIONICOLIDAE (ACARI, HYDRACHNELLAE) FROM AUSTRALIA

by Kuer O, Viets*

Summary

Viers, KO. (1980) New Unionicolidae (Acari, Hydrachnellue) from Australia. Trans. R.

Soe. §. Aust. 104(2), 27-40, 29 February, L980,

Seven new species of the water mite genus M/nieantcala, subgenos Pentama (Acari,

Hydrachnellne), are described from Australian freshwater mussels: OUniericola (Pentatax)

walkeri nap. U. (P) procursa op. UO. UPL) assimiliy ap, U, CP.) conjunetella nsp,, U.

(P.) ligulifera tsp, Us CP.) clipeata fusp. and U. (PL) seurdta nsp, A further tew species

is placed in Unionirolapsis oplmipalpis n.g., n.sp.

Introduction

The Hydrachnellae are prostigmate Acari,

Within the family Unionicolidae Oudemans,

1909 there are five subfamilies: Encentrito-

phorinae Viets, 1935 (20 spp, from Africa,

Australia, southern Asia), Najadicolinae

Viets, L935 (one sp., North America), Piona-

tacinace Viets, 1916 (many spp., world-wide),

Pollicipalpinae Viets, 1914 (two spp., Africa)

and) = Utonicolinae Oudemans, 1909, ‘The

Unionicolinae include four genera: Umionicola

Hakleman, 1842 (many spp. world-wide),

Vietsutax Uchida & Imamura, 1938 (one sp,

Japan), Hererati® Lamdblad, 1941 (one sp.

Africa) and Atacella Lundblad, 1937 (six spp.,

South America).

The taxonomy of Unionivela and its asso-

ciated subgenera still is somewhat unsatis-

Tavtory, but is based on the numbers of

genital ucetabulae, the appearinee of the

genital ficld. and the sexual differentiation of

the legs of males, The diagnoses of systematic

groups above subgenert) were last summarized

hy Cook (1974), Species of the subgenus

Jionicold 3.8. possess six pairs of genital

acetabulag: (wo species are known fron Aus-

Iralia, Species of the subgenus Pentatas Thor,

1927 have five pairs of acetabulae; three Aus-

tralian species ure known.

Some species of Unionicola are free-living,

others parasitic for part or all of their lite

cycle (ea, im molliises, Viets & Plate 1954;

Mitehell 1955; Hevers. 1978, 1978h). The life

histories of most species, however, are un-

known, In Australia, One L/iinnicola species

only has been reported in association with a

freshwater mussel, namely U. (U/.) clrrosa

Koenike 1914, in the mussel Unio nepeanensiv

(syn, (yridella enstraliy (Lamarek)),

Although the precise locality in Australia is

® Friedensir, 4B, D-2940 Wilhelmshaven, West

Germany:

unknown. the host mussel is likely to have

come from a coastal stream in the southeast

of the continent (cf, MeMichacl & Hiscock

1958),

Recently f obtained collections

mites from various Australian freshwater

mussels (Hyriidae) through Dr Ko Bb, Walker

of the University of Adelaide; [aim grateful to

him and the other collectors. Dr Walker also

adapted this manuscript from the original

German. rom the material seven new species

of Unlonicola, subgenus Pentatax are described,

and Unionicolopsis na, is erected for an

udditional new species.

of Watcr

General Remarks

The types und paratypes deseribed herein

are catalogued i the Viets Collection (Wil-

helmshaven), and ultimately will go to the

Senckenberg-Museum, Prankfurt.

The legs of water mites are 6-scamented: |

trochauler, 2 basifernmur, 3 lelolemur, 4 gent,

§ tibia, 6 larsus. The legs and their segments

usually are symbolized as, for example, first

les tarsus; 1.1.6 and fourth leg tibiar PV,L,5

(see Cook 1974: Fig. 5). The pulps are 5-

segmented: | trochanter, 2 femur, 3 genu, 4

tibia, 5 tarsus. These are denoted P FV (Cook

1974; Pig. 6),

All measurements herein are jim.

Unionicola (Pentatax) walkert rsp.

FIGS 1-8

Holorype 2 prep. 6638; With soft miegument,

In dorsal integument le two pairs of delicate,

oblong plates (muscle attachment sites), an-

terior pair nearer one ahother than the pos-

terior puir; length 35-50,

Coxal area (Fig, 2) 415 long, Third coxae

wonsiderably sherler in mid-line than fourth

coxac; suture between coxal pairs does not

28 KURT QO. VIETS

50m

Figs 1-8, Unionicola (Pentatax) walkeri n.sp. 1. 2 holotype prep. 6638, IV.L.5—6, right; 2. ? holotype,

ventral side: 3. 2 holotype, 1.L.5-6, left; 4. ¢ prep. 6675, I.L.5-6, right, dorsal aspect; 5. @ holo-

type 6638, right palp; 6. ¢ allotype prep. 6642, left palp; 7. d allotype prep. 6642, genital field; 8.

® holotype prep. 6638, genital field.

NEW UNIONICOLIDAE FROM AUSTRALIA 2

reach medial margin. Posterior margins of

fourth coxae rounded, and cach wilh pos-

teriorly-directed process. Medial margin of

third ant fourth coxae 198 long,

Genital field (Fig, &) entirely at poslertor

end of body. It consists of two pairs of

medially-constricted plates; witernor pale each

Wilh two genital acetubulae, and posterior pair

each with three acetabulac, On strongly-

lapered) medial edge of each anterial plate

short, stout sela (stylet), and neac it

smaller, slender seta, On medial edge of each

posterwr plate large. thiek, curved sela, and

alongside two (in some cases three) slender

setae, Gonopore (about 182 long) surrounded

hy pre and post-genital sclerites.

Capitulum (Fig, 2) 162 long, ¢, 104 wide.

Chelicerae similar ti those of other Uaionl

volu species. Dorsal palp segment lengths (left

PI-V): 10, 105.53. 109, 54, P Il on each

side with bwo selne, and PLE one seta, P TV

has no ventral process, apart fram a minute,

often indistinet, peglike seta at its distal end.

PV ends in two strange claws,

Legs LIV with number of ventrally-attached

setae, On seament 5 of all legs, and On segment

4 of legs If and VV, are 3 long. slender swine

iing-setae (el Cook 1974: Big, 5), located

distally, Last segment of leg 1 (Pigs 3-4),

seen fram side, strongly expanded distally (.c.

dorsd-vertrally expanded) to form laree claw

fossa, On dorsal side, at distal end of segment,

slender-based, spnon-shaped, chitinous struc:

jure, In Ply. 40 tuesal claws omitted, Club-

shaped structure situated on distal ead of TV.L.6

(Fig. 1). Small, spoon-shaped seta attached

near tarsal claws on UL.6 and 1.1.6. Tarsal

claws simple in form, having no carpus, hur

with slender, terminal spine. Dorsal segment

lengths af legs Pand Ws LL.3-6: 74. 115 -

97. VIR IV.LGe6: 94. 155, 180, 165,

Alleotype & prep. 6642: Coxal area Clength

410) and dorsal side correspond closely with

& Genital field located terminally as an en-

closed plate 127 long wind |45 wide. Por ar-

rangement of genital acetabulae and hair

pores. see Fig, 7,

Cupitulum 149 long and e. 100 wide. Palps

(Fig. 6) similar to 9, lefi P L-V, measured

dorsally, as follows: 11, 97.. 54. 105 , 53.

Leys similar to 9%) dorsal segmentdensths:

Lbh3a-6; 70, 11). 99. 114: INLD: 92,

146, 17, 152,

Vorivrion- coxal area, leneth 415-453 P27),

480143 4409) gonopore, length incl, selerites

169-188, , genital ficld ¢, length =, T14—

127; genital field ¢, width ,,., 124-165; eapitu-

jum, length 162-177, 143-159; capitulum,

wilth 103-114, 91-101: chelieera, length

(152), (135-152); palp, dorsal segment length

PL K-13, 7-11. P UE 99-113, $2-105: Poot

46-62, 47-59; BP IV 109-120, 100-LI4: P VW

53-58, 44-57; jews, segment length 11.3 74—

84, G9-7h; LI4 114-124, 103-119; LT.5 95-

107, 89-105; [LL.6 110-122, 104-1215 1V.1.3

94-104, 83-99; IV,L.4 155-170, 135-158:

IV.L.5 177-198, 157-182; IV.L.6 165-175,

I46—159; egg, long axis 135-143,

Jats aml lovulities GUNS, Austad: Alathiyria jack

sont Iredale, Lock 3, River Murray, KF. Walker,

19.x.1977 (1 o&\ TL 9, holotypeys Lock 3, R.

Murray, K. F, Watker, 5.411977 (1 @y allotype)>

Velesunio wakicuus (PHU pO, Lock 3, R. Murray,

K. EF. Walker, 19.47.1977 (8 & 7 9)y Point Sturt,

Lake Alexandrina (R. Murray) K.P. Walker,

30.x,1977 (4 9); L. Alexandrina nr Milang,

M, C. Geddes, 20.41,1977 (3 ¢, 2 9): Point Sturt,

L. Alexundrina K, &. Walker, 3.811977 (30, 2 9).

Unionicofas (Pentatax) procursa n.sp,

FIGS 9-14

Nololype & prep. 66712 Dorsal integument and

vosal area (Fig. 9) very similar to Lf. (P,)

Walkeri nap, although posterior process of

fourth coxa somewhat shorter, Coxul area 446

long.

Genital field (Fig, 10, lat, view) at end of

body, In dorsal aspect (Fig. 11) jbdominal

integument at anterior margin of field indented

(although this is not clear fram Fig, 10),

Anterior plites of genital field, eaeh with twa

atetabulue, directed posteriorly, Bach atterior

plate with two stout setae ul hindimost cx-

Iremity, Posterior plates broader, and bear one

seta at the ends of their respective posterior

processes.

Capitulum 150 tong and 14 wide an-

leriorly. Chelicerae like those of congeners,

Long, slender P V (Fig. 12). and, as with re-

lated species, two distinct terminal claws. P

IT) with two setae on outer horder, and three

inner setac. Dorsal sczment lengths (lefr P

VW): 15. 110. 60. 116. 73,

116 similar to that of UL CP.) walkeri nsp,

(Fig. 13; tarsal claws omitted for clarity). It

is, however, smaller and the distal border of

the expanded part of the large chiw fossa is

vonvesly rounded, nat strongly indented as in

other speetes, Large, spoot-shuped appendage

30 KURT QO. VIETS

Figs 9-14. Unianicola (Pentatux) procursa n, sp. 9. 9 holotype, prep. 6671, ventral side; 10. 9 para-

type, prep. 6673, genital field, lateral view; 11. 2 holotype, genital field; 12. 2 holotype, left palp;

13. 2 holotype, 1.L.5-6, left; 14. ¢ allotype, prep. 6676, genital field.

on LL.6 like that of U. (P.) walkeri nsp.

Stout seta on dorsal side of IT and III.L.6,

proximal to cach claw; tends to a spoon-shape

on leg Ll, but simple on leg III. No club-

shaped chitinous structure on end of IV.L.6,

as in related species. Otherwise leg setation

shows no significant differences, Dorsal seg-

ment lengths: 1.L.3-6: 95 . 163. 117 . 129;

IV.L.3-6: 104 . 168 . 183 . 167.

Allotype 3 prep. 6676; d and 2 very similar,

Coxal area 365 long. Genital ficld (Fig. 14)

differs from other species in form and

especially number of hair-pores, A small an-

terior projection, 114 and 126 wide dorsally.

Capitulum dimensions 122 : 85. Chelicerae

126 tn length. Palps as in 2; dorsal segment

lengths (left P I-V): 14. 94.50.100. 64,

Legs as in §. Dorsal segment lengths: 1.L.3-6:

78, 124 , 92.. 109; IV.L.3-6: 82.130. 139.

144.

Variation: coxal area, length 365-393 dd (4),

405-446 29 (5); capitulum, length 122-133,

135-150; capitulum, width 83-90, 94-104;

palp, dorsal segment length P [ 12-14, 13-16;

P If 90-100, 98-110; P IIL 44-51, 51-64; P

TV 101-105, 112-119; P V 59-67, 64-73;

genital field (9), length 114-120, |; genital

field (3), width 126-137, . ; legs, segment

length LL.3 75-80, 88-97; LL.4 121-128,

144-164; LL.5 92-99, 105-117; LL.6 105—

109, 115-129; IV.L.3 79-85, 92-108; 1V.L.4

129-139, 149-169; IV.L.5 139-151, 164~-183;

NEW UNIONICOLIDAE FROM AUSTRALIA 31

Figs 15-19. Unionicola (Pentatax) assimilis n.sp. 15. 2 holotype, prep. 6625, ventral side; 16. 9 holo-

type. left palp: 17, 9 holotype, I.L.5—6, left; 18. ¢@ paratype, prep. 6635, dorsum; 19. ¢ allotype,

prep. 6633, genital field.

IV.L.6 137-146, 161-168; egg, long axis,

160-163.

Host and localities (all S, Aust.): Felesraio anm-

biguas, R. Murray nr Mannum, K. F. Walker.

19.x1.1977 (1 o&): Point Sturt, L. Alexandrina (R.

Murray), K. F. Walker, 30.%.1977, (5 @): L.

Alexandrina nr Milung, M, C. Geddes, 20_xi.1977

(74. 1 9. inel. holotype and allotype); Point Sturt,

L. Alexandrina (R. Murray), K. F. Walker,

3.4i1,1977 (5 2).

Unionicola (Pentatax) assimilis n.sp.

FIGS 15-19

Holatype © prep. 6625: Ridged posterior plates

of dorsal integument (Fig, 18, 4) about 130

Jong. Coxal area (Fig, 15) length 406. As in

the other species, suture between the third and

fourth coxae does not reach medial margin,

and is directed transversely. Genital field, capi-

tulum and chelicerae similar to U. (P.) pro-

cursa nsp. P HW (Fig. 16) bears two setae on

inner and outer sides. P V ends in two claws;

length in same proportion to P IV as in other

species. Dorsal lengths of P If and P IV nearly

identical, whereas in U. (P,) procursa o.sp.

P TV is slightly longer than P Tl. Dorsal seg-

ment lengths (left P I-V): 11. 105 . 50.

103. 61.

LL.6 (Fig. 17) expanded distally, and

52.6-62.7% of segment length; it is also

shorter in proportion to I.L.5 (90,5-101.2% )

than is the case for U. (P.) precursa n.sp.

(106.5-118.5% ), 1.1.6 bears a spoon-shaped

distal projection like the other species. On

11.L.6 and HI.L.6, however, only one stout

seta at distal end of dorsal edge, and this is

not spoon-shaped. Dorsal segment lengths:

1.L.3-6: 84 . 136 . 95. 90; IV.L.3-6: 90.

144 . 172 . 149,

32 KURT ©, VIETS

Allorype 3 prep. 6633: Dorsal integument,

coxal area, palps and legs similar to ?, Pos-

terior dorsal plates about 115 long, with strong

chitinous ridge (Fig. 18), Coxul area length

355, Genital field (Fig, (9) about 80 lone and

97 Wile, weakly indented al anterior border,

Capuulum dimensions 132 = 749. Dorsal palp

segment lengths (left P LV): — , — . 42~

85, 54. Dorsal leg segment lengths: I.L3-6:

74. 110, BS. BIS 1V.1. 3-6: 75. 123, 150

134,

Fariation: coxal area, length 344-480 cd (6),

dill 442 29 (6); posterior dorsal plate, length

105-137, 125-140; eapittilum, length 124-138,

143-157: capitulum, width 76-85, 94-100;

cheliverae, length (102), (125-132); palp.

dorsal segment length PT 10-12, 10-13; PH

85—97, 102-112: P TIL 42-48, 50-62; P 1V

82-89, 99-110; P V 50-54, 56-67; genital

field (), length (77-85), 3 genital fleld (4),

width 89-108, + leg, segment length 1.0.3

65-83, 84-98; E.L.4 104-119, 136-145; LS

77-89, 95-105; LL.6 75-85, 89-97; 1V.1.3

7I-84, 89-97; TV.L.4 115-132, 144-155;

IV.L.5 142-160, 172-186; IV.L,A 130-139,

147-165; egg, long axis =, (133-138);

Host and locality: Wextralunia cartert: Tredale.

Murray River S of Dwellinuup, W. Aust, N. M.

Morrissy, [5.xi1.1977 (8a, 13 9, 11 nymphs, ingl

holorype und allotype),

Remarks: Allied to U. (P.) procurya wasp.

Significant differences between the two species

are summarized in Table |.

Unionicola (Pentatax) conjunctella n.sp.

FIGS 20-25

Holotype 2 prep. 6669 Dorsal side (Pig, 23,

a) like that of U (P.) assinills asp. Ridged

plates (c. 135 long) very thin, outline not

always eVident. in contrast to ridge itself,

Coxal area (Fig, 20) 360 long. Suture between

third and fourth coxae rims obliquely, ap-

proximately parallel to anterior margin of third

coxae, and fused with medial edge of posterior

plates. Genital flekt (see Fig. 20) similar to

other species.

Capitulum {42 long and 87 wide, abd, like

the chelicerae, with no distinctive characteris-

tics. Palp (Fig. 21) segment P IL bears two

sefac on cach of its inner and outer sides,

PBorsal lengths of segments (left P I-V): 12.

89, 42.91 .—.

L.L.6 (Fig. 22) similar to that of U, (P.)

assimilix n.sp, Terminal segments of legs I and

Ht each with expanded spoon-shaped seta

dorsally, at distal end, in front of tarsal claws,

Dorsal segment lengths: 1.L.3-6: 64.93. 72.

76; IV.L.3-6: 77.115 , 140, 125.

Allotype 3 prep, 6663: Dorsal side (Pig. 23)

similar to 9, Length of posterior plates 158,

Coxal area 386 long, Unlike 9, first coxae (Fig,

24) extend posteriorly beyond ends of Outer

apodemes. Genital field 94 long and L110 wide,

(Fig. 25) ke U. (P.) asvimilis n.sp.

Capitulum 140 long and 8&7 wide. Palps

similar to 8; dorsal segment Jengths (left P

1-V): 10.93.45. 93. 47, Legs ulso similar

to ?. Dorsal segment lengths: I,L, 3-6; 66 ,

99.76. 80; 1V.L.3—6; 77, 119. 147. 132.

Variation: coxul area, length 340-406 det (7),

320-380 99 (4); posterior dorsal plates, length

130-158, 130-135; capitulum, length 125-145,

124-142; capitulum, width 76-90, 80-87;

chelicera, length (110-125), (115); palp,

dorsal segment length P | 10-13, (12); PW

79-97, 83-89; P [1 37-47, 40-45; P IV &4—

98, 84-93; P V 43-48, 42-47: genital field

(3), length (81-94), | =: genital field (<*),

width 107-129, |; legs, segments length 1.1.3

57-71, 58-64; LL4 85-105, 85-04; LL

TAbies |, Comparison af U. (P.) assimilis and U, (P.) procursa

U. (P.) assimilis nes.

U. (P.) procursa n.sp,

dorsal inteminient

ment sites;

subire between Goxae J and 4 Lransverse

venirul field (4)

P 1 mner side 2 setae

Li.6 => broad

inex, wlth os & segment ;

le twits od: $4.3-83.7%

R9> 52.6-60,0%6

1 pair small ant. musele altach-

Lo piir post. plates

with strony ridge

Without medisl process; post, 4

with many hait-pores

| pair small ant. muscle attuch-

ment sites; L pair post. plates

without strong ridge

oblique, << parallel to

border of 3rd coxa

with medial process; post. 4 with

few hair-pores

3 setae

> slender

ant,

ad: 40,2-41.3%

O- 36,8-40.0%

NEW UNIONICOLIDAE FROM AUSTRALIA 33

\ :

23 st”

Figs 20-25. Unienicola (Pentatax) conjunctella n.sp. 20. 2 holotype, prep. 6669, ventral side; 21, 2

holotype, left palp; 22. 9 holotype, I.L.5-6; 23, ¢ allotype, prep. 6663, dorsum; 24. ¢ paratype,

prep. 6662, coxal area; 25. ¢ allotype, genital field.

66-83, 66-76: LL.6 71-88, 72-77: IV.L.3

69-87, 70-77; IV.L.4 105-129, 108-121;

IV.L.5 131-155, 136-148; IV.L.6 120-143,

117-131; [.L.6, maximum width 43-50, 44—

47: egg, long axis — , (165).

Hasts and localities: Alathyria jacksoni, Lock 3,

R. Murray, S. Aust, K. F. Walker, 19.xi.1977

(1 @): FKelesunio ambiguus, R. Murray nr Man-

num, S. Aust, K. F. Walker, 19.xi.1977 (2 2,

1 2); Lock 3, R. Murray S. Aust., K. F. Walker,

19.1x.1977 (3d, incl, allotype, 1 %); Rocklands

Reservoir, Vict.. P. J. Suter, 20.x1.1977 (1 et);

Point Sturt, L. Alexandrina (R. Murray), S. Aust.,

K. F. Walker, 30.x.1977 (1 ¢ holotype).

Remarks; Distinguished from U. (P.) precursa

n.sp. and U. (P.) assimilis n.sp. in that suture

between third and fourth coxae extends to

medial margin of posterior plates.

P V is considerably shorter than in other

species, as seen in comparisons of P V length

as % PIV length (fo + 2): U. (P.) conjune-

tella n.sp. 46.2—-53.6%; U. (P.) procursa n.sp.

57.1-65.7%; U. (P.) assimilis nsp. 56,0—

64.3%.

Unionicola (Pentatax) ligulifera n.sp

FIGS 26-32

Holotype 2 prep. 6664: As with U. (P.) con-

junctella u.sp.. dorsally two separate, thin

plates with prominent chitinous ridges. Coxal

area (Fig. 26) 373 long. First coxae do not

extend beyond posterior ends of apodemes,

Suture between third and fourth coxae short

and does not reach medial margin, Genital

ficld (Fig. 27) like that of other species except

U, (P.) walkeri n.sp.

34 KURT 0. VIETS

Figs 26-32. Unionicola (Pentatax) ligulifera usp. 26. 2 holotype, prep. 6664, coxal area, left: 27.

4 salons genital field; 28. 9 holotype, left palp; 29. 2 holotype, I.L.5—6, left; 30. 2 holotype,

1.L.5—6, left; 31. ¢ allotype, prep. 6666, coxal area; 32. ¢ allotype, genital field.

NEW UNIONICOLIDAE FROM AUSTRALIA 35

Capitulum dimensions 120 : 81. PTT (Fig.

28) hears two setae on inner and outer sides.

PV long, 57-58%r of PIV length, Dorsal seg-

Ment length Cleft P HV)5 12, 85.44.91,

52.

L.L.6 (Fig, 29) shorter than 1.L.5 and typi-

cal of other species in the Pentatax group, i

and HLA (big, 30), like 1.1.6, auch with a

large spoon-shaped chitinous structure distally.

Species in relaled groups have, on these seg-

inents, Minute setac only slightly expanded

distally, Dorsal segment lengths: 1.1.3-65 72.

TTR, 100. 89: 1V.L.3-6:-85 . 134. 152. 1399.

Allatvpe 3d prep. 6666 (+ paratype a, in tote);

Dorsal integument similar to ?, Coxal afea

(Pig. 31) 332(326) long (paratype dimensions

in parentheses), First voxwe slender in mid-

posterior region and wide and elongate wh ex-

Iremily, Genital field (Fig. 32) 134 wide.

Foremost four adetabulae om cither side

arcanged i rows,

Capitulum 103(102) Jong and 70(69) wide,

Palps as in 2; dorsal segment lengths Clete P

I-W)s WNT2) . TITEL. 34037), 7777)

45(45). Legs similur to Y. Dorsal segment

lengths: 11,346: 59.97 , 87, 78; IV.L,3-6:

73 110, W322. 117,

Aloxsty and ftocaliiwa Alaiiyrta jawksarni, Lock 3,

Ro Murray, So Awash, KR. oR. Walker, 19.97.1977

(1 4th) Velesunia ambiewas, Lock 3, R, Murray, 8.

Aust, Ko B Walker, 1941977 (1 2, 2 of nel,

holotype and ulloty pe)

Remarks: Distinelive ip that UU, and ULL 6

tach bear, on their distal-dorsal mareins. a

large. spoon-shaped chitinous structure similar

to that borne on 1.1.6 Although in the & the

first coxae do not extend beyond the posteriar

upodemes, they are very long in the ef

markedly longer than in the ¢ of U. (P.) cen-

funetella nap, The prajcetion extends to the

suture between the third and fourth coxae, The

suture does not reach the medial margin of

the postermm plates.

Unionicola (Pentatax) clipeata nisp.

FIGS 33-38

Holorpe So prep. 6647 (paratype @ prep.

6649); (Measurements of paratype in paren-

theses). Weakly chitinized, undivided dorsal

shield has dimensions: 202(18B8) 180(171).

Cosal area (Pig. 33) 302(271) long. First

coxae do not extend beyond posterior end of

apodemes, Suture between third and fourth

coxac curved over entire Jenygth, und meets

medial mmirgin of posterior plates. Fourth

coxae have almost right-angled medial-

posterior margin. Genital field (see Fig, 33)

similar to preceding species.

Capitulum dimensions 112(95), 6760),

ehelicerye &7 long, P IL (Fig. 34) has two

sclac on inher and outer sides. Relative length

of P V between that of LL (P.) ceonjunerella

nsp, und &, (P.) proeirsa nsp, Dorsal seg-

ment lengths (left P I-V)> 1108), 60055) .

36(29) . 66(63) — 38(33).

11.6 (Fig. 35) relatively short and wide

(61,3-67.2% of segment lengih), and with

convex distal margin. Distal-dorsal setae on

legs [1 and If only slightly expanded, Dorsal

leg segment lengths: Ef3-6; 51(48)

7O0(68) ~53(52) . 61(59) 5 1V.L.3-62 59055) -

89(86) , 1O7(106) . S4(96),

Allatype & prep. 6648 (+ pararype & prep.

6650): Dimensions of dorsal shield (Fig. 36)

208 : 178, Coxal area 288(280) long, similar

to 2. Genital field (Fig, 37) with many bair

pores, indented anteriorly and 127(132) wide.

Capitulum 99 long and 63 wide, Palp dorsal

segment lengths (left P I-V):—(8) . S8{359) -

32(30) . 62(61) . 36(33); Lews similar to ¥.

Dorsal segment lengths: L1.3-6: S051)

H9(70) . 53054) - 6261), 1IV_L.3-G: 56058) -

R2(86) , 105(103) . 95(96),

Hast and localicv: Welesinia ambieuys, R, Murray

hr Mannum, S, Aust, K. F, Walker, (9.xi,1977

(2 3,2 9) inch holotype and allotype).

Unionicola (Pentatax) scutata n.sp,

FIGS 39-45

Holetype ? prep, 6679; Dorsal shield (Fig. 39)

aboul 280 long and finely pored. On each side

small, weakly chitinized shield, with hair

pore, in front of anterio’ muscle attachment

sites, Coxal area (Pig. 40) 366 long. Suture

between third and fourth coxae extends to

medial margin of posterio’ plates, First coxa

does pot extend beyond end of posterior

apodemes. Genital field (see Fig, 40) similar

to other specics,

Capitulom 114 long and 74 wide. PU (Pig.

41) with 2 setae on inner and outer sides. Bor-

sal segment lengths (left P FeV): 13. 68 , 35

Sl, 40,

1.L.6 (Pig. 42) similar to other species: as

with U. (P.) elipeata n.sp., slightly longer than

penultimate segment. Distal-dorsal setae on ET.

and HhL.6 only slightly broadened (cf, spaon-

shaped), IV.L.6 (Fig, 43) has, in the middle

of its distul extremity, vlub-shaped chitinous

siticture comparable to 0. (P.) walkeri nsp.

36 KURT O. VIETS

36 “ow >

Figs 33-38. Unionicola (Pentatax) clipeata n.sp. 33. 2 holotype, prep. 6647, ventral side; 34. 2 holo-

type, left palp; 35. 2 holotype, I.L.5—6, left; 36. ¢ allotype, prep. 6648, dorsum; 37. ¢ allotype,

ventral side, posterior; 38. ¢ allotype, left palp.

Dorsal leg segment lengths: I.L.3-6: 55 . 88.

65 . 64; IV.L.3-6: 66 . 110. 138 . 123.

Allotype & prep. 6680 (+ paratype ¢ prep.

6681): (Dimension of paratype given in

parentheses). Dorsal side similar to 2. Coxal

area (Fig. 44) 333(375) long. First coxae

extend beyond end of posterior apodemes (in

these characters the ¢ is similar to the d of

U. (P.) conjunctella n.sp.). Genital field (see

Fig. 44) 138(158) wide, and posterior margin

(Fig. 45) indented; large numbers of hair-

pores in posterior area.

Capitulum 109(118) long and 70(75) wide.

Palps are similar to 2; dorsal segment lengths

(eft P I-V): 8(9) . 60(70) . 30(33) .

72(77) . —(41). Dorsal leg segment lengths:

IL.L.3-6: 55(58) . 85(89) . 64(67) . 67(68);

IV.L.3-6: 62(67) .

116(121).

Host and locality: Velesunio angasi (Sowerby),

Ja-Ja Billabong, Magela Creek, Arnhem Land,

N.T., W. D. Williams, xi.1977 (2 o, 1 9, incl.

holotype and allotype).

Remarks: Like U. (P.) clipeata n.sp., this

species has an undivided dorsal shield in which

borders have become fused. Essential

differences between the two species are in

Table 2.

Genus Unionicolopsis n.g.

Diagnosis (based on 2 only): With soft integu-

ment. Coxae in four groups, the posterior

group especially widely separated; anterior

coxal group without posterior apodemes. Geni-

tal field with delicate, weakly chitinized plates,

102(110) . 128(136) .

NEW UNIONICOLIDAE FROM AUSTRALIA 37

Figs 39-45. Unionicola (Pentatax) scutata n.sp. 39. 2 holotype, prep. 6679, dorsum; 40. 2 holotype,

ventral side; 41. @ holotype, left palp; 42, 2 holotype, I.L.5—6, left; 43. 2 holotype. [V.L.5-6, right;

44. ¢ allotype, prep. 6680, ventral side; 45. ¢ paratype, prep. 6681, genital field.

body size

dorsum

genital field

IV.L.6

KURT O. VIETS

TABLE 2. Comparison of U. (P.) scutata and U. (P.) clipeata

U. (P.) scutata n.sp.

large (330-380)

dorsal shield strongly chitinized; with a

pair of small shields, each bearing hair-

pore, in front of ant. muscle attachment

sites

with many hair-pores

with distal club-shaped structure

U. (P.) clipeata n.sp.

small (270-300)

dorsal shield weakly chitinized; without

shields in front of ant. muscle attach-

ment sites

with few hair-pores

without distal club-shaped structure

Figs 46-53. Unionicolopsis opimipalpis n.sp. 46. 2 holotype, prep. 6683, ventral side; 47. 2 paratype,

prep. 6684, genital field; 48. 2 paratype, prep. 6682, genital field; 49. 2 holotype, capitulum, lateral

view; 50. 2

left palp; 53. 2 paratype, prep. 6684, leg IV, left.

paratype, pre. 6682, capitulum, dorsal view; 51. 2 holotype, chelicera; 52. 2 holotype,

NEW UNIONICOLIDAE FROM AUSTRALIA 39

anterior plates cach with two, posterior plates

cuch with three, genital acetubulae. Medial

margins of plates without special spines or

setae, Capitulom with broad upper processes,

Pulp stout, without process on P LV.

Type species. Unlonicelepsis opimipalply asp.

Unionicolopsis opimipatpis n-sp,

FIGS 46-53

Holotype ® prep. 6683 (+ paratype 22 preps-

6682, 6684): In soft dorsal integument is pair

of Jong and pair of short muscle atlachment

siles; these are not significantly chitinized, and

not formed us plates, Datu for all three speci-

mens are given (paratypes in parentheses).

Third and fourth coxae (Fig 46) relatively

widely separated in medial line; medial length

about L48(145, 148), Posterior apodemes of

first coxal group absent.

Genital plates (Figs 47-48) very weakly

chiunized, and indistinct in outline; widely

separated, on both sides of gonopore (c. 165

(165, 175) long). As in Pentatay, each an-

terior plate with two genital acetabulae, and

posterior plates with three acctabulae, Nuniber

of avetabulae may vary (Fig. 48),

Capitulum (Figs 49-50) stout, abour 164

(150, 163) lone and —(119, 120) wide, and

ends posteriorly in two wide-lobed, upper

processes. Chelicerae 165 long (Fig, 51),

Palps stuut (Fig, 52), P I with two setae on

inner and outer sides, No process on P IV, P

V ends in two large, dissimilar claws.

Legs very simple in form. On 1.0.3, in about

middle of ventral side, is conspicuous, very

long, strong seta, and beside it a short seta,

On T1.L.3 and 4 is distal seta and another

proxinmully. Sctae on segment 3 dissitnilar int

length, Whereas those of segment 4 are about

equal, and in general longer than those on

seoment 3, At distal extremity of WLL.S paw

of sete (V.L.1 hears three distinet setae (Fig

53); all other segments of leg IV with only

very small spine-like setac. Seements 4-6 on

leg TV elongate, and segment 6 slightly cliirved,

All tarsal claws simple. Dorsal leg segment

lengths: LL, 3-6: 59(59, 62) . 75€67, 75) .

72065, 72) . T5€7S, 79); IV-T.38-6> 109199,

105) _ 169(L58. 173) . 187(179, 199) — —

(154, 164).

Flost and lacalis Velesunio ambleans, Ry Murray

ur Albury. SSW, T, 2. Hillman, xi,1977 (3

incl, holotype).

Remarks’ Only 3 29 of this new species jire

available and, because the 2 remains unknown,

the systematic position of the material is un-

certain, Whether the new species, for which

the Unionicolapyty ng. wow is efected, should

be placed as a subgenus in Uniertieala, must

remain in doubt pending discovery of the ¢.

It appears unlikely ta me.

List of mussels and associated mites

Alathyria jackson] Wedale: U, (P,) walkeri,

conjunctella, ligulifera.

Felesanio ambiguus (Phillipi)s Of CP)

walkeri, conlunctella, lizulifera, precursa, ell-

peala; Unianicolopsis apimipalpis.

Velestinio anger (Sowerby)! U, UP) setitata.

Westralunia carter’ Wedale: U. CP.) avsimiilis,

Key to the species of the Pcoutaisx group

described herein

|. Dorsum with undivided shield, with pair of

distinct chitinous ridges

Dorsum without complete shield 3

Shield strongly chitinized; IV.L.6 with distal

club-shaped chilinous structure; first coxae of

§ falling short of, those of ¢ extending beyond

posterior apodemes seule

Shicld weakly chitinized: 1V.L.6 without distal

club-shaped chitinous structure; first cosas of

Cand @ not extending beyand poslerior apu-

demes clipeuta

3. Dorsum with two weakly chitinized plates,

euch having disunet chitinous ridge 4

Dorsom without chitinized ridges, hut with

muscle altuchment sites On weakly chitinzed

plates. 6

4. Sulure between third and fourth coxaé Teach-

ing medial murgio of posterior pair af plates;

distul-dorsal edges of IT, and ULL. with only

slightly cxpanded (spounshaped) seta; first

coxue of ® shorter than those of @, longer than

postetior apodemes confunerella

Sature between third and foutth coxae nat

teaching medial murgin of pesteraae pair of

plates a (Wie heetie

5. Th and W1,L.6 with setae Only on distal-dorsal

margin: first coxue of ¢ and % not eatending

beyond posterior apodemes nssiinilis

U. and W.6 with large spoon-shaped chiti-

nous simucture dorsally (as on LLG): first

coxae of 9 shorter (han, and hose of ¢@ extend-

ing bevond posterior apodemes teaching

suture between third and fourth coxae)

livutifera

6. P Vv long (57, 1-65. 19% of P TY Tength); inner

ale of PEL with 3 setae, IV L.6 without elub-

like structure ; procurse

PV short (45,7-41,9% of P TY length): inner

side Of P WE with 2 setae, LV.L.6 with elub-like

structure (? genital field distinct from that of

other species, with 4 similar plates and short,

ifick spines) Pcie nrenKcn . walkers

40 KURT O. VIETS

References

Coox, D. R. (1974) Water mite genera and

subgenera. Mem. Amer. Ent. Inst. 21, 7

860 p.

Hevers, J. (1978a) Zur

Gattung Unionicola (Hydrachnellae,

Zool. Jb. Syst. 105, 33-64.

(1978b) Morphologie und Systematik der

in Deutschland auftretenden Schwamm-und

Muschel-Milben-Arten der Gattung Unionicola

(Acarina: Hydrachnellae: Unionicolidae). Ent.

Generalis, Stuttgart 5, 57-84.

KOENIKE, F. (1914) Neue und _ neubenannte

Wassermilben. Abh. naturw. Ver., Bremen 22,

383-404.

Sexualbiologie der

Acari).

MITCHELL, R. D. (1955) Anatomy, life history

and evolution of the mites parasitizing fresh-

water mussels. Misc. Publ. Mus. Zool. Univ.

Michigan, Ann Arbor 89, 1-28.

McMicuwaEL, D. F. & Hiscock, I. D. (1958) A

monograph of the freshwater mussels (Mollusca:

Pelecypoda) of the Australian region. Aust. J.

Mar. Freshwat. Res. 9, 372-507.

Viets, K. & PLATE, H. P. (1954) Die okologischen

(parasitologischen ) Beziehungen zwischen

Wassermilben (Hydrachnellae, Acari) und

Sufwasser-Mollusken. Z. angew. Ent., Berlin

35, 459-494,

VOL. 104, PARTS 3 & 4 30 MAY, 1980

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Twidale, C.R. The Devil’s Marbles, central Australia - - - - - 41

Breed, W. G. Further observations on spermatozoal morphology and male

reproductive tract anatomy of Pseudomys and Notomys species

(Mammalia: Rodentia) - - - - - - - 51

Flint, R. B., Ambrose, G. J. & Campbell, K. 8. W. Fossiliferous Lower Devonian

boulders in Cretaceous sediments of the Great Australian Basin 57

Beveridge, I. Progamotaenia Nybelin (Cestoda: Anoplocephalidae): new

species, redescriptions and new host records - - - - 67

Mawson, P. M. Beveridgea new genus (Nematoda: Strongylida) from the Agile

Wallaby from northern Australia - - - - - 81

Ludbrook, N. H. Non-marine molluscs from dolomitic limestones in. the north

of South Australia - - + - - - = 2 83

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

THE DEVIL’S MARBLES, CENTRAL AUSTRALIA

BY C. R. TWIDALE

Summary

The Devil’s Marbles consist of castle koppies (catellated inselbergs) and large residual boulders,

both developed in granite. They are exposed in the core of an anticline outlined topographically by

bevelled sandstone ridges. The major granite forms developed in two stages. Fracture-controlled

differential compartment weathering beneath a late Mesozoic land surface was followed by stream

incision and the erosion of the weathered bedrock. In this way the resistant essentially unweathered

compartments and blocks were exposed and left in relief. The landscape in and near the Devil’s

Marbles is almost entirely the result of the erosional exploitation of the differentially weathered

bedrock. The residuals are thus of etch character.

THE DEVIL'S MARBLES, CENTRAL AUSTRALIA

by C. R. PwipaLt*

Summary

‘Twipace, C. R. (1980) The Devil's Marbles, central Australia, Trans. R. Soc. §. Aust. 10403),

41-49, 30 May, 1980,

The Devil’s Marbles consist of castle koppies (catcllated inselhergs) and large residual

boulders, hoth developed in granite, They are exposed in the core of an anticline outlined

topographically by bevelled sandstone ridges. The major granite forms developed in two

stages, Frocture-controlled differential compartment weathering beneath a late Mesozoic land

surface was followed by stream incision wnd the erosion Of the weathered bedrock, In this

way the resistant essentially unweathered compartments and blocks were exposed and left

in relief. The landascupe in and near the Devil's Marbles is almost entirely the result of the

erosional exploitation of the dilferentially Weathered bedrock, The residuals are thus of etch

chirticter,

The massive, simple, granite forms, largely lacking intricate fretting and sculpture, are

typical of humid tropical regions rather than lemperate lands, and stand in marked contrast

with most of the granite landform ussemblages of southern Australia.

Introduction

Though not as dramatic, large or famous as

Ayers Rock and the Olgas, the groups of re-

sidual granite boulders known collectively as

the Devil's Marbles are nevertheless well

known and constitute a considerable attraction

for tourists Visting central Australia. Located

asinde the Stuart Highway about 50 km south

of Tennant Creek, the residuals lie within

200 kin of the geographical centre of Australia

in central Mount Stuart (Fig. [) and with an

average wnnual rainfall of some 350 mm (13.7

itches) per annum are situated within the

tropical semiarid zone of the continent.

Residual granite bowders are by no means

rare, Granite comprises about 15% of the con-

tinental areas and apart from planation sur-

faces, boulders are the most common landform

development of such outcrops, The Devil's

Marbles are however unusual by virtue of ihe

size of the boulders, their arrangement, and

their detailed morphology. Many of the resi

dual houlders are 11-12 m in diameter and at

several sites these giant blocks stand im orderly

arrangements so that they look tike the rem-

nants of Cyclopean masonry (Fig. 2). ‘Vech-

ically they are castle koppics frather than

tors—see Twidale 1971), Other large holders

ure precariously perched either on other blocks

or boulders or on rock platforms: others stand

in pairs, one on the other, fo form cottage

loaves; yet others have split in two us iF sliced

by some gigantic cleaver (Pig. 3).

* Department of Geography, University of Ade

luide, Box 498, G.P.O. Adclue, 5. Ausr. S00),

General setting

The granite on which the boulders are deve-

loped is a coarse-grained grey porphyritic. mus-

covite-biotite adamellite, with large phenocrysts

of feldspar, Radiometric (K/Ar) determina-

tions give an age of about 1510 ma, ic. the

granite is Lower Proterozoic (Smith 1974).

Tt intrudes Hatches Creek Group sedinients,

also of Lower Proterozoic age (Smith 1974)

and is exposed in the core of an asymmetrical,

plunging, anticlinal structure involving these

sedimentary strata (Fig. 1). The structure is

expressed topographically in a V-shaped out-

crop of sandstone Which is part of the Daven-

port Ranges and which borders the granite to

hoth north and south, The sandstone ridge is

bevelled, 1t stands some 490 m above sealevel

and 70-80 m above the eastern lower valicy

floor, though only 30-40 m higher than the

plains at the harrow western end of the low-

land.

On the southwest the granite oaytcrop is

drained by the headwaters of Sutherland Creek

which flows south through a gorge in the sand-

stone fudge, but the greater past of the enclosed

anticlinal valley drains north by way of Dixon

Creek and its tributaries. The axial stream of

the drainage system is situated at the western

end of the Valley und is in fact followed by

the Stuart Highway. The major part of the

granite outcrop lies east of the Highway so

that there is a general decline in the altitude

of the granite surface from east to west, The

main groups of boulders are exposed near the

Highway in the lowest pari of the valley,

42 C. R. TWIDALE

Central _™@

Mt Stuart

= AL ge

Devils?”

Marbles

: upland surface (Early Cretaceous)

(probably pre-silcrete)

‘upland ridges in Proterozoic

sediments, with strike shown

plain in sediments

mesa in weathered granite

plain cut in granite, with

occasional residual boulders

Okm 3

_ high plain cut in granite

“= (slightly weathered)

groups of large residual boulders

(tresh)

Fig. 1. Morphological map of Devil’s Marbles and environs. Location map inset.

though there are others scattered over the

plains (Fig. 1).

The surrounding hills and plains provide as

much evidence concerning the evolution of

these huge balls of rock as do the boulders

and blocks themselves, and for this reason

they are considered first.

Planation surfaces

Plains of low relief are quite extensively

developed on the granite outcrop and indeed

occupy a far greater area than do the residual

boulders. There are also remnants of two

higher surfaces of low relief (Figs 1, 4).

The present plain is rolling or undulating

and is shallowly dissected by numerous stream

channels, It is eroded in granite that, though

hard and cohesive is nevertheless weathered:

the potash feldspar is generally white due to

clay mineral alteration, the biotite is partly

altered to chlorite, and there is abundant frac-

turing both along grain boundaries and across

grains, Iron staining is obvious in thin section.

The cut bedrock surface is covered by a few

THE DEVIL’S MARBLES, CENTRAL AUSTRALIA 43

. ‘ ‘ ; i a. ' _-

fi - i ie _ = —- |

i a te ns 1 ‘ =. ~~

s iA

Fig. 2. Castle koppie in Devil’s Marbles complex consisting of massive quadrangular blocks, most in

situ. The residual rises above valley floor beyond which is sandstone ridge with markedly bevelled

crest,

>, - =

| <n < : 7

e.. . -

Rahs, i ,

Meee ee ie SN tinned ano b8 .

Fig. 3. Split boulders at Devil’s Marbles. Parallelism of fractures is noteworthy. Fractures can be

traced through several boulders some tens of metres apart.

44 C. R. TWIDALE

high plain (granite) summit surface

sandstone

midslope platform

“ar- Pe ine om - >

Rien

SX SS SANA

RRS - = =

vo sf ‘ses —_ gpm» _— — ——_—___— —_—

met tae as tension

zone of fe

fluctuating ft neutral plane

water level :

compression

Fig. 4. Diagrammatic cross-section through Devil’s Marbles and adjacent areas.

Fig. 6, Field sketch of granite high plain and matching platform cut on slope of sandstone ridge,

Fig. 7, Two-stage development of Devil’s Marbles. Dots indicate weathering.

THE DEVIL’S MARBLES, CENTRAL AUSTRALIA 45

centimetres of granite sand (quartz with frag-

ments of feldspar and mica). Near the sedi-

mentary outcrops at the margins of the plains

small plates of sandstone are a_ significant

constituent of the regolith, and in the vicinity

of the few ridges underlain by quartz blows or

reefs, white vein quartz is also abundant.

Small boulders and blocks stand above the

general plain level in several areas. Their lower

slopes are commonly roughened and fretted, or

pitted (see Twidale & Bourne 1976), indicat-

ing recent, possible local, lowering of the soil

surface of 20-25 cm. In addition the major

granite forms known as the Devil’s Marbles

rise from this plain (Figs 1, 4).

Quite extensive remnants of a higher plain

are preserved on the granite (Figs 1, 4).

Bounded by rudimentarily faceted slopes up

to 5 m high, this high plain carries a thin

discontinuous veneer of granite sand. Granite

platforms, with residual boulders and blocks,

are also present. The granite exposed in this

high plain is more weathered than that beneath

the present plains. The potash feldspars are

white due to partial kaolinisation, while the

plagioclase has been strongly altered to an

orange-brown clay, identified as kaolinite prob-

ably discoloured by goethite, The rock is ex-

tensively fractured as a result of weathering

and iron oxide and clays are commonly found

both in fissures and along crystal boundaries.

Standing 25-30 m above the high plain are

three mesas capped by highly weathered

granite. Quartz and muscovite are the only un-

weathered minerals, though the latter is altered

along its cleavage. The rock samples appear

to differ from the main mass of the outcrop

and to be a greisen or primarily altered granite.

The feldspars are completely altered to a

brown orange kaolinite (again probably with

goethite) which also fills intergranular spaces.

The residuals are bounded by faceted slopes in

which coarse blocks of granite are exposed

(Fig. 5).

Both high plain and mesas can be correlated

with planate features preserved on the sand-

stone ranges. Though standing a few metres

lower, the mesa surface with highly weathered,

a 7 ee i 4

96% ae

aT wan ents

Fig. 8. Parted block at Devil’s Marbles,

46 Cc R, TWIDALE

though still cohesive, granite can nevertheless

reasonably be related th the prominent summit

hevel of the Davenport Rasiges (Figs 1, 4, 5).

The tigh plain has ils counterparts in a dis-

Unct platform developed and preserved at

midslope on the inward-facing escarpments of

the sandstone ridges (Fig, 6). Thus the land-

scape around the Devil’s Murbles is multicyclic

in character. Each of the two lower surfaces

is contiguous over wide areas, und the three

display different degrees of hedrock weather-

ing; they are not identified solely on thy basis

of relative elevation.

Mabbutt (1967) has referred the summit

surface of the Davenport Ranges on what he

ealls rather slight palacogeographic evidence.

to the later Mesosme. This supguestion tinds

support in equivalents of the surface in the

Barrow Creck and Alice Springs aves standing

higher, and being therefore older, than silerete

remnants of carly-mid Tertiary ave (Wopfner

& ‘Twidile 1967), The bevelled ridges of the

Devil’s Marbles region also stand higher than

lateritised surfaces to the north, and as these

also are of early-rmid Tertiary age (Stewart

1954; Twidale 1956; Hays 1967), the later

Mesovoic age of the summit surface ix cor

roborated. The summit surface is in fact part

of a later Mesozoic land surface of Jow relief

ihat has been reported from several parts of

tropical and sublropcal Ausiralig (see eg,

Woodard 1955; Twidale 1956, 1966, 197fa,

198%; Wright 1963; Mabbutt 1967; Hays

1967),

This summit surface and tts eqyivalent in

the mesas developed on granite is the datum

to which the formation of the residual boulders

can be referred, for all of the Devil's Marbles

ogeur below it (Fig. 4), It is a weathering

surface that has suffered leaching, strong

kaolinsation above the weathering rimt or

lower limit of significant weathering (Mab-

butt 1961), and precipitation of tron oxtdes

near pnd For some metres below this level.

Major granite forms

hat the summit surlace itplics a period of

relative standstill and weathering of the wader,

lying bedrock is demonstrated by the altered

ytanite preserved in the mesas. Had the granite

been homogencous there would have beer imi

form weathering beneath the plains surface,

but the bedrock is jointed wnd altheush he

cause of erosion it 1s nat possible ty discern

what joint patterns bad developed in the

srinite bencath the contiguous stuninit surface,

there jire indications that fracture spacing

varies both Verteally and laterally. For ex-

ample whereas the joint harks in some of the

Wore prominent residuals are 10-12 m in

diameter the joints exposed in creek beds

nearby are only 20-30 cm apart. Again, the

large residuals stand on plinths that are even

MOre Missy.

Observations in many parts of the world

Suggest very strongly that granite is subdivided

ito massive and well-jointed compartments.

The latter are readily and rapidly westhered

while the former remain intact. As the land

surface is lowered the weathered rock is

eroded, leaving the stillefresh and cohesive

compartments in relief, as residuals the size

and shape of which depends on fracture pat-

tern (Fig, 7). ‘Thus it is argued and has been

urged for almost two centufies (see Hassen-

fraty 1791; Logan 1849, 185): Mennell 1904;

Twidale 19784) that the granite residuals

evolve in two stages, one involving differential

joint-controlled subsurface weathering, the

other the differential crosion of these unequally

weathered compartments (Linton 1955); Biidel

1957; Wilhelmy 1958; Twidale 1971; Ciodard

1977)

In the case of the Devil's Marbles, differen-

tial comparttient weathering look place he-

neath the late Mesozoic fand surface repre-

sented by crestal bevels. preserved on the

sandstone ridges and hy mesa remnants. The

differential subsurface weathering took place

during the later Mesozoic and carly Cainozoic

when this region, like the remainder of central

Australia, was warm aod humid to subhumid

(Kamp 1978), The exposure of the koppies

and boulders, on the other hand, is. a later

Cainozoie event probably related to regional

warping and resultant stream rejuvenation

In these terms the castle koppies arg com-

parltnents characterised by widely spaced sets

of orthogonal joiuts, though the flat-lying joints

afe almost certainly either the Luverklifte of

Cloos (1922) of sheeting joints (Gilbert 1904;

‘l'widule 1973), The residual boulders are large

cerestones or kernels remaining after the

marginal weathered zones of the joint blocks

Wave been ered, The perched blocks and

coltuge loaves are to some extent fortuitous,

though lyecause weathering advanecs down

from the surface it can be expected that more

residuals Will Survive at depth than closer to

the surface. sa that in some places isolated

blocks will come to stand on broader bases

(Pig. 7).

THE DEVIL'S MARBLES, CENTRAL AUSTRALIA +

The present plain ig related to present local

baselevel (Dixon Creek) wnd undoubtedly re-

Meets aw lowering of baselevel compared to

later Mesozore (Surimit surface) times, The

high plain however could cither be an ctch

surface or exposed weathering front (Wayland

1934). or jt could be related to a baselevel

intermediate between the summit surface and

the present plains, The former interpretation

appears the more likely, for the variations in

veanite weathering appear ito be part of a single

profile rather than ovo or more. The platforms

previously noted (Fig. 6) on the inward-facing

sandstone ridges, and toterpreted as extensions

of the high plain stirface, could be of stimtlar

elch type and due to particularly intense

moisture atfuek i ihe then scarp foot zene

Thouth the high plain slopes down to the west,

the weathering front was probably irregular

ii detail because of variations in joint spacing

and glso because of ihe slope of the wuter

lable to the major water courses. The blacky

upstanding koppies and large boulders, which

were presumably once surrounded by well-

jointed weathered rock, also stam on much

broader, plinths or platforms of massive

cranite-compartments thar survived to a inuch

preater extent than thase above them because

they remained beluw the weathering front

(Pig. 7).

Thus. the major Jondforms of the Devil's

Marbles are readily comprehensihle in terns

of the two-stage cofeept. The residual rem-

nants, though angular, probably represent

dome structures developed as a result of com-

nvession in the erust (ef, Denham ef al, 1979),

They have been modified by aggressive

weothering ot depth and at the margins of the

massive conioartnients, Where ground waters

persist. and in contrast with the near-surlace

dner, or seasonally dry, zones,

The minor forms

The boulders, blocks, and large-radius

dornes are fretted and seulptured in detuil,

though the resultant modifications are in most

instances minor, Some blocks and particularly

some of those high on residuals are bath in

Preenated with jron and manganese oxide and

creally fretted and hollowed (alveolar weather-

ing}, Polygonal patterns of surface cracks are

developed in these impregnated zones, These

weathering phenomena argue the presence of

water and the zones of intense attack may be

related to former fluctuating water tables. On

the other hand similar intense fretting is found

at some sites at the bases of blocks and

houlders, close to the old weathering front,

and spain abundant water is suggested as the

reason for the especially aggressive weathering.

Some Jarge boulders are clongate and

streamlined and are called whalebacks or doy

de baleme. A few large blocks have seemingly

moved laterally telalive to one another (Pig.

8), rather like the purted blocks deserihed

front Dartmoor (Worth 1953), Many blocks

are split into two parts (Fig, 3), Some

secondary joints have heen exploited by

weathering to form shallow straight grooves

(Kluftéarren), though there ure on some

domes true Rille (Echikarren) due to stream

erosion, Some of them are coated with a black

compound, consisting of carbon plus oxides of

iron and manganese (Francis 1921). Similar

coatings On granite occur in former pools in

creck beds, indicating that this black material

has been deposited fram water. These black

colours arc however, unusual, for virtnally all

of the residuals catry a patina of reddish-

brown iron oxide which etfeetively masks the

grey colour of the granite seen in ereek beds

and where there has been fire flaking, Sealing

of the rock surface is peneral, and pitting, due

to differential weathering of surfuce crystals

leaving quartz in microrelie! has been noted

on lower slopes, Rock platforms in places dis-

play regular patterns of vertical joints so that

the whole looks like a pavement, Al some sites

the joints are weathered and there are minor

flared slopes developed in the sidewalls of the

clefts so formed,

Basal fretting has already been referred to

and some boulders display poorly developed

flared slopes. A fow basal tafoni have been

noted, but it is because of the virtual ahsence

of this and other forms (flates, enammas or

weather pits, gutters or Rille) that the Marties

stand in such contrast with granite exposures

in southern Australia (see Twidale 1971,

1976b; Twidale & Foale 1972).

The origin of most of these minor land-

forms is well known and ts adequately dis-

cussed elsewhere (Wilbelmy 1958: Twidale

1971, 1976b; Twidale & Poale 1972: Twidale &

Bourne 1975),

Several lines of evidence point to the minor

forms having been initiated by moisture attack,

in the subsurface, at the weathering (rant, Tn-

ciplent pitting, fared slopes, platforms, tafoni,

saucer-shaped depressions and gutters have

been observed already developed on the hed-

rock surface when the rogolithie cover was

48 c. R. TWIDALE

stripped away and some forms, particularly

Rille. can be traced into the subsurfyce

{Logan [851, Twidyle 1962, 1971, 1976),

1978b; Boyé & Fritsch 1973; Twilale & Bourne

1975, 1976, 1977), The cover 1s weathered

granite in situ, not introduced material, so that

there is no question of the minor Jealures

developed in granite having been formed on

exposed surfuces and then buried, The forins

are modified—either developed or destroyed —

aller exposure, but they are initiated in the

subsurface.

Only three of the minor landforms call for

further brie! comment. First, with reward to

parted btteks, Worth (1953) rightly dis

counted gravity, for the blocks stand ow fut

or Very gently sloping inclines. lee vr nivel

action can be discounted at the Devil's

Marbles, and shaking by earthquakes seems

Wolikely, for not only is the area siesmically

quiet hut had there been carth tremors suffi-

cient to dislodge the parted blocks, no perched

hontders would strely have survived.

Second, split rocks have been attributed by

several writers lo healing and cooling under

desert vonditious (e.g, Hume 19275; Hills

1975), Tt is very doubtful whether this pro-

cess alone, or even aided by ihe cooling effect

of rain showers, could achieve the splitting of

such massive bodies of rock. Furthermore split

rucks are even more common in pival revions

fee. the Pyrenees) than they are in arid areas.

It is suggested that three factors are involved,

Though the houlders and bloeks thar are split

we basically defined by orthogonal joints, it

is a matter of Observation that many inclide

ofher, presumably secondary or latent joints

(Fig. 3), These subsidiary [ractures are ex-

Ploited by weathermg processes and notably

by walerio either liquid or solid form, depend

ing oon climatic conditions. Finally arnce

weathering has sufficiently affected the subsr,

diary fracture and provided tt ts vertically ar

near-vertically disposed, the weieht of the twa

halVes will cause the weakened fracture to be

pulled apart, so creating the split rack.

Third, polygonal erackine is clearly net a

primary rock feature ws sugeested by some

writers (Johnson 1927; Leonard 1929), for i

is developed on boulders whieh are Lhemselyves

the product of differential subsurface weather-

ing At Devil's Marbles and iw the Pilbara

of Western Australia it Nas been aoted thal

polygonal cracking is mssocialed with rock that

is heavily impreenated with iron and oian-

ganese oxides, In the Pilbara, near Mount

Magnet and oo Eyre Peninsula the cracking

frequently affects two or Mose superiniposed

Jayers of rock, and some of the plates de-

lineated by the cracks are arched slightly

upwards, Various mechanisms have been cone

sidered and found wanting. The most likely

is thal salts of iron and mangunese which are

mobile are carried in groundwaters and pie-

cipitated out near the weathering front, Le-

near the margins of the boulders whilst they

are sull corestones and beneath the land sul:

face. The continued precipilation of salts

causes the buckling of the rock in the direction

of least resistance, namely outwaris and We

fracturing of the shells into polygonal plites.

Lastly it is emphasised that the Devil's

Marbles are simple groups of residual boulders.

lacking any greal variely or development of

minor forms. With regurd te the latter, the

forms that are absent, or virtually so, are as

interesting ws those that are present. Thus,

flared slopes, tafani, Rifle and rock basins are

rare or poorly developed. In this respect the

Devil's Marbles are more akin ta the tropical

granite cxposures of northwest Qucensland,

the Pilbara and the Darwin area rather than

those of the temperate, particalarly the Medi

lerranean environments of much of South Aus-

tralia, southern Victoria and the Wheat Belt

al Western Australia. This is oot ta sugpest

either that flared slopes for instanee are not

found in the northern areas (though they are

rare and poorly developed there) or that they

have evolved to a spectacular degree on all

southern outcrops, Many factors are mvolved

and in many respects it is not a simple ques-

ion of development or pon-development, but

rather of degree of development und preser-

vation, Nonetheless, zoned contrasts are dis

cernible and the Devils Marbles both in gross

and in detail have more affinities with the

frumid tropics than with the tempetate and

Mediterrancan lands of southern Australia.

Acknowlevlgments

The author wishes to thank Dr A. R. Milnes,

C.S.LR.0. Division of Soils, for notes and

comments on various petrographic samples,

and Liz Campbell for support in the fleld. The

field work was carried out with the aid of an

award from the Austrulidg Research Grants

Crmrieniitec

THE DEVIL'S MARBLES, CENTRAL AUSTRALIA 49

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FURTHER OBSERVATIONS ON SPERMATOZOAL MORPHOLOGY AND

MALE REPRODUCTIVE TRACT ANATOMY OF PSEUDOMYS AND

NOTOMYS SPECIES (MAMMALIA: RODENTIA)

BY W. G. BREED

Summary

Spermatozoa of Notomys cervinus have a head with three hooks, whereas those from N. fuscus are

variable but have only two very short hooks. Spermatozoa from Pseudomys forresti, P. fumeus, and

P. gracilicaudatus all have a head with three hooks. Only one very short hook occurs in P.

novachollandiae, and there are no hooks in spermatozoa from P. delicatulus, P. shortridgei has a

spatulate sperm head with a large acrosome. Insertion of the sperm tail is lateral in novaehollandiae,

offset basal in P. delicatulus and mid-basal in P. shortridgei. Principal and end pieces are shorter in

the last two species.

FURTHER OBSERVATIONS ON SPERMATOZOAL MORPHOLOGY AND

MALE REPRODUCTIVE TRACT ANATOMY OF PSEUDOMYS AND

NOTOMYS SPECIES (MAMMALIA: RODENTIA)

by W, G, Breen*

Summary

Breen, W, G. (1980) Porther observations on spermatozoal morphology and male reproductive

tract anatomy of Psendomys andNolomys species (Mammalia: Rodentia). Trans, 2. Soc. 8,

Aust. W4(3). 51-55, 30 May, 1980,

Spermatozon of Notomys cervinus have a head with three hooks, whereas those from

N. fuseus are variable bul have only two very short hooks, Spermatozoa from Pseucdormys

farrestl, P. fumeus, and P, gracilicaudatas all have a head with three hooks, Only one very

short hook occurs in P. norachollundiae, and there are no hooks in spermatozoa from P-

delicatulus, P. shortridgei has a spatulate sperm head with a large acrosome, Insertion of the

sperm til is lateral in P. novachollandiae, ollset basal in P, delieatulus and mid-basul in

P, shorirideei. Principal and end pieces are shorter in the last two species.

Notamys alexis, N. fuseus, and N, mitchellii have very small testes, whereas lhey are

relatively larger and scrotal in N. cervinus. In the first three species seminal vesicles and

congulating glands are vestigeal or non-existent, whereas in N, cervinus they ore well developed

and weigh up to 150 mg, The possible phylogenetic and functional significance of these

differences is discussed.

Introduction

Phylogenetic relationships between different

species of rodents have been investigated by

a variety of techniques, all of which have at

least some limitations. In several groups of

North American and British =myomorph

rodents spermatozoal morphology and cum

parative anatomy of the male acecssory sex

wands have been used (Friend 1936, Bishop &

Walton 1960, Arata 1964, Linzey & Layne

1969, 1974), The latter uuthors concluded

that in Peromyscuy Variation in accessory sex

glands corresponded well with major taxo-

nomic groupings based on other criteria,

whereas variation in spermatozoal morphology

did not coincide with the subgeneric eroups,

Breed & Sarafis (1979) extended a brief report

by Illison (1971)1; investigated spermatozaal

morphalogy and male reproductive tract ana-

tomy in some species of Australian Todents,

and discussed phylogenetic relationships he-

lween Various genera. They found that within

each genus similar spermatozoal morphology

oceurred apart from Noatamys. Wison (1971)!

reported that Pserdomys shurtridged has a

primilive sperm type, and P. delieatuluy (as

Leeeadina delivatila) a spermatozoal head

with no books, so it appears that Pseudontys

~ Department of Anutomy and Histology, Vni-

versity of Adelante, GPO. Box 498, Adelaide,

S. Aust. S001,

7 HHlison, by Abstract of paper presented at Aust

Martitnal Soc. Meeting val. 2, No. 8, Dee, 1971,

exhibits considerable spermatozoal diversity;

all five species that we investigated had a

sperm head with three hooks. Male accessory

sex glands were generally similar between the

genera investigated, apart from the two species

of Notomys which differed markedly (Breed &

Satafis 1979), Here spermatozoal morphology

of six other Preudwrys and two other Notontys

ypecics is presented, together with an examina-

tion of the male reprodnetive tract from all

four Notoennyis species,

Materials and methods

Spermatozoa were obtained fram single

adult male individuals of the following species

housed ut the Institute of Medical and Veter-

nary Science (1,M.V,S,), Adelaide,

Netomys cervinus: Boru al University pf NLS.W,,

received JWIV.74; N, fuscus; Laboratory bred at

IMVS,, Peevdomys delicatulys! collected at

Shortcut Rd, Nourlangie, NOT. ChM.Y.S. publ,

1017): P, forrestiz received trom University of

N.S.W,, 10.1V.79 (1M,V,S, publ. 953)5 PF. faerneus:

from Arthur Ryluh Institute, Melbourne (1.M_V,S

publ. 952); P. gravilicavdatus: (rom School of

Biological Sciences, Macqtiarie University

(LM.V.S, publ, 950); FP. shortridgei: from

Fisheries and Wildlife Division, East Melbourne

(1.M.Y,S, publ. 951),

In all individuals a small incision was made

into the region of the tail ol the epididymis

under halothane anaesthesia. and a small bi-

apsy taken. Spermatoyea were then squeezed

onl onto microscope slides previously Mouded

52 W. G,

with glutaraldehyde/formaldehyde/ picric acid

fixative (see Ito & Karnovsky 1968). Semi-

permanent mounts were made by placing a

coverslip on top of the sperm and ringing the

mount with DePeX. Subsequently the sperm

were photographed with Nomarski optics at

CSIRO Division of Horticultural Research,

Glen Osmond. Measurements were made of

several spermatozoa from each species under

phase contrast using an eyepiece micrometer

as described by Breed & Sarafis (1979), Al-

though difficulty was experienced in obtaining

accurate Measurements, the mean values for

head length, midpiece, and principal together

with endpiece were determined.

Adult male individuals of Netomys mitehel-

lit, N. alexis, N. cervinus and N. fuscus col-

lected in the field (1960-1978), preserved in

formalin or 70% alcohol, and lodged at the

S.A, Museum, W.A. Museum or 1.M.V.S.,

were Weighed. A single testis, seminal vesicles

with coagulating glands, and ventral prostates

BREED

were dissected out, cleared of adherant fal,

subsequently weighed and, where appropriate,

measured. The testis weight was subsequently

doubled to give the approximate weight of

paired testes. A few laboratory bred adult

Notoniys held at 1.M.V.S. or Medical School,

University of Adelaide, were also killed and

tale reproductive tracts dissected out and

weighed. A single N. cervinus (provided by

Mr R, Briggs) was weighed, dissected and in-

vestigated similarly.

Results

Table 1 and Fig. | present morphological

details of spermatozoa determined by light

microscopy. Sperm of P. forresti, P. fumens,

and P. gracilicawdatusy had a head with three

hooks, although the size of the sperm head

and length of hooks was greater in P, gracili-

equdatus. The sperm head of P. novaehol-

landiae had a single short top hook and a

truncated or non-existent lower hook, That of

Fig. 1. Spermatozoa. A:

principal piece, ac

Pseudams gracilicuudains; B: funteus; C: P. forresti: D: P, novaehollandiae:

E: P. delicatulys; B: P. sheriridgei; G: Notoniys cervinus: A: N. fuses. mp == middle piece, pp =

acrosome, cd = cytoplasmic droplet.

OBSERVATIONS ON SPERMATOZOAL MORPHOLOGY 53

TaBLE 1: head and tail length of spermatozoa from various Notomys and Pseudomys species.

Species Average size of spermatozoa (um)

Principal and

Head Midpiece endpiece Total

Notomys fuscus 7 22 77 106

N. cervinus 9 26 80 115

Pseudomys delicatulus 4 19 65 88

P. forresti 7 26 95 128

P. fumeus 8 20 100 128

P. gracilicaudatus 10 21 98 129

P. novaehollandiae 6 22 78 106

P. shortridgei 5 22 69 96

P. delicatulus had no hooks and was smaller

than the others. P. shortridgei also had sperm

with no visible hooks. It was spatulate in shape,

and a large acrosome occurred over the

nucleus. The principal and endpieces were

shorter in the last two species.

Notomys fuscus had variable sperm head

morphology, but usually there were very short

and truncated top and lower hooks. N. cer-

vinus sperm had a head with a long top hook

and two lower hooks united at their base.

In wild caught N, alexis testes weight ranged

from a mean of 20-37 mg with time of year.

Often no obvious scrotum was discernible.

Seminal vesicles were at most only just visible

in the preserved material and did not exceed

3 mm length. Coagulating glands and dorsal

prostates were vestigeal or non-existent. Large

ventral prostates occurred which varied in

weight during the year; no seasonal trend was

apparent. Laboratory bred adult N. alexis have

similar reproductive tract anatomy (Breed

1979, Breed & Sarafis 1979).

Similar male reproductive tract morphology

occurred in N. mitchellii and N. fuscus (Table

2). By contrast, that of N. cervinus was

markedly different (Table 2, Fig. 2). The

testes were relatively larger and scrotal in posi-

tion, although adult body weights were similar

to the other species. Conspicuous seminal

vesicles and coagulating glands were present;

their average weight being about 130 mg and

length about 10 mm.

Discussion

The suggestion by Breed & Sarafis (1979)

of intrageneric differences in spermatozoal mor-

phology and male reproductive anatomy in

Pseudomys and Notomys has been confirmed.

Most Pseudomys and two of four species of

Notomys have spermatozoa with three hooks.

In P. novaehollandiae there appears to be only

one short truncated hook, and all three hooks

are missing in spermatozoa from P. delicatulus

and P. shortridgei. Preliminary transmission

electron microscopy (TEM) has confirmed a

large, somewhat eccentrally placed, acrosome

Fig. 2. Male reproductive

tracts. A: Notomys

mitchellii; B: N. cervinus. t = testis, sv =

seminal vesicle, vp — ventral prostrate, cg =

coagulating gland, vd = vas deferens,

54 W. G. BREED

TApte 2; Adult reproductive organ weights of male Natomys (mean + S.E.)

Si pe ee a a ag

Seminal

Ventral vesicle &

prostrate coagulating

No. of Bady wt Testis wt wr gland wt

animals (g) (mg) (meg) (mg)

Notomys alexis

Fixed tissue

Month of capture

Jan & Feb 6 20744 22+4 62 + 26 —_

Mar & Apr 16 30+ 0.5 31+6 8426

May & June 19 30+3 37 +4 77+9

July & Aug 18 3043 22+3 5542

Sept & Oct 4 3143 3021 125 +30

Noy & Dec 3 37 tee 31+11 98 + 26

Fresh tissue 7 3 28+ 2.6 38 +3 8948 —_—

ide 4 29+72 3329 97 +20

Noatomys mitchellii

Fixed tissue 13 392+2 50+ 3 162+ 21 —

Fresh tissue 3 48+ 2 Jx47 407 + 223

Notomys fuseus

Fixed tissue 9 2842 4344 5817 =

Natomys cervinus

Fixed tissue 12 3842 133 +8 WoH7 130421

(10 + 0.7) #####

Fresh tissue 1 32 170 103 150

(11) ##4*

* Vestigeal or non-existent: maximum length of seminal vesticlaes — 3 mm,

j¥ From Breed 1979 (80 days of age).

*** Brom Breed & Sarafis 1979,

atch Body wt of only one animal recorded.

*#24> Length of seminal vesicles (mm) given in parenthesis.

in P, shortridgei, and a few cup-shaped cya-

ginations in the apical part of the nucleus, In

P. delicatulus the acrosome appears consider-

ably different and somewhat complex in struc-

ture,

TEM has also shown that the connecting

piece of the tail in P. shortridgei hag a mid-

basal insertion into the sperm head, an offset

basal insertion in P, delicatulus and a lateral

insertion in P. nevaehollandiae and other

species with the more typical sperm head mor-

phology. N, fuscus, N. alexis, and N. miitchellii

all appear to have somewhat variable sperm

head morphology and the former two species

truncated. or nonexistent, hooks (see also

Breed & Sarafis 1979).

Most non-Australian murid rodents inyesti-

gated have a sperm head with a single top

hook (vide Friend 1936, Bishop & Walton

1960), whereas most species of Australian

rodents have sperm heads with at least two,

and usually three. hooks (Illison 1971, Breed

& Sarafis 1979). It seems plausible that some

ancestral, non-Rattus, murid rodent evolved a

sperm head with this complex structure, and

that adaptive radiation of the group within

Australia then occurred, most species main-

taining this specialised sperm head morpho-

logy. The reduction, or lack of, hooks in the

few Notomys and Psendomys species is, there-

fore, probably a recently derived state. Varia-

bility in sperm head morphology in the twa

Notemys species with truncated hooks may

support this contention.

The anatomy of the male accessory sex

organs of Pseudumyys investigated is similar.

regardless of the differences in spermatozoal

morphalogy, There are relatively large ‘leaf-

like’ seminal vesicles 6.5 mm or more in length

in P. gracilicaudatus and P. australis (Taylor &

Horner 1972), P. hermannshurgenesis (Taylor

& Horner 1970), P. apodomoaides, P. forrestt,

P, novaehollandiae, and P. delicatulus (Breed,

unpublished). Taylor & Horner (1972) state

that no coagulating glands follow the pasterio-

lateral contour of the seminal vesicles in P.

OBSERVATIONS ON SPERMATOZOAL MORPHOLOGY as

australis, but that in laboratory-bred animals

such glands were found, and the mixing of

secreuens Of seminal vesicles and coagulating

glands results in the occurrence of hard gela-

fines material. Vaginal plugs, which in com-

mon laboratory rodents result feum a mixture

of secretions from sentinal vesicles and coagu-

laling glands (Mann 1964), have been fe-

corded in laboratory bred PL aistrelis (Smith,

Watts & Crichton 1972),

In Notomy'y considerable inter-specifie dif-

ferences occur in accessory sex gliml and

testicular development. N. cervinus has the

typical complement of male actessary sex

alands, whereas in the other species the seminal

vesicles, couguluting glands. and dorsal pros-

states are vestigeal or non-existent, No cervinns

is also the only species of Netomys for which

a vaginal plug has been treeorded (Crichinn

1974) and it also has typical serorul testes,

wheres they are relatively much stiller and

perisnal in position iw the otbers, Lack of

testicular development presumably results im

the absence of an obvious scrotum thal often

aceurs if these species.

The above findings jndivate, therefore, thal

spermatozoa and the mule accessory sex alanis

are samewhat labile structures, as considerable

variation occurs within Netumys that, on other

morphological and physiological groynds, ap-

pears to be a discrete and closely related group.

Since N- cervinus bas the more vonventional

pattern of male reproductive tract anatomy, the

occurrence of the vestigeal glands, very sriall

testes, and the apparent lack of vaginal plug

formation in the other three species is likely

to be a recently derived state. The tunetional

significance of these differences hus yet to be

elucidated, but it may be significant that rela-

tive testis size appears to correlate with senvinal

vesicle and coagulating gland development

Perhaps in species With relatively small testes,

fewer sperm ure produced, stored, and thus Te-

leased at ejaculation, Less energy, and there-

fore seminal fluid, would thus be required for

ther metaholism in the female ceproduclive

tract, This, in turn, may result in atrophy of

sume of the glands involved in the production

of seminal Huid. Why such divergonee should

evolve in a closely related group of species ts,

al present unknown, bul a study on the sexual

and social behaviour of these animals is being

carried out, and this may shed some light on

the significance of these observed anatomical

differences.

Acknowledgments

1 thank Drs P. Baverstock and C, Watts for

enabling me to obtain sperm from their

animals, Dr D. Kitchener {W.A. Museum)

und Mr P. Aitken (S.A, Museum) for allow-

ing me access ty material, and Mr Ro Rriggs

for the donation of a single Notonrys cervinter,

l also thank Br A. Bird, C.S.LK-0, Division

ol Horticultural Research for permitting me

to use his Nomarski microscope, and Mr R.

Murphy, Mr C, Leigh, Mrs G. Hermuanis, Mr's

|, Brazier and Mrs B, Sheldon for assistance

in the Department of Anatomy,

Referenees

Arata, A. A, (1964) The anatomy und roxena-

mic significance of (he male accessory reprodiic

tive lands of curl rodents. Aull, Florida State

Mus. 9, 1-42-

Baverstoce, P,, Warts, ©, HOS. & Hoar, 1 'T,

(1977) Chromosome evolution in Austeallan

rddenis. | ‘The Pseudomyinae, the Hydromyinue

and the Uromys/Melomys group. Chromosoma

Gi 9§-(25.

Aisin, M. 'W. EL & WaAtron, A. (1960) Sperma-

tovenesis and the structure of mammalian

spermatozoa, Claptor 7 in A. S, Parkes (Fd.

“Marshall's Physiology of Reproduction” Vol,

112) fLongmans, Tondon).

Bheep, W. G, (1979) The reproductive rate of

the hoppine-mouse Nelamys alexis and is ecea-

logical significance. Anse. J, Zaol. 27, 177-94,

& Sansers, Voo61979) On the phylogenetic

significance of spermainzoal morphology nnd

male renraduerve tract anutomy in Australiuin

rodents Trang. 2, Sac S, Anse, U3, 127 035-

Crician, Fo. (1974) Aspects of reproduction

ii the genus Veron (Muridae), Aust, 4, 200,

22, 439.447_

Fauienp, G- F. (1936) ‘The sperm of British muri-

dae. Quart. #, Micros, Sei, 78, 419-443.

Tro. S & Karnovsky, M. 2.17968) Formaklelyde-

wlutaraldehyde fixatives containing dinitra come

pounds, J. Cell Biol. 9, 168A-169A.

Linzky, A, Vo & Layne, I, N. (1968) Compare

tive morphology of the mile reproductive tract

in the rodent genus Perenmyscus (Muridwe)

Aimer, Mus, Navir, (2355), 1-47,

—— (1974) Comparative morphology of sperma-

tozog of the rodent genus Peraeyaruy (Muri-

dace), Thid, (75324 1-20. :

Mann, T, (1964) “The biochemistry and semen

uf the mule reproductive tract.” Methoen, Lune

on.

Suma, TR. Warts. C. HOS, & Cemcrox, EG

(1972) Reprodoction in the Australion desert

rodents Nofomwys alexts and Psencdanive aystea-

lis (Muridne). dusr, J. Mamearol, 1. 1-7,

Tayiorn, J M & Horner, BOR, 11970) Observa-

tions on reoraduction in Leevadinw (Rodentn.

Miridne) SL. Agammral $1, 10-17,

_— (1Y72) Observations on the reproductive

Hulowy of Prydemys (Rodentia) Mirtidac).

(hid 53, 318-428

FOSSILFEROUS LOWER DEVONIAN BOULDERS IN CRETACEOUS

SEDIMENTS OF THE GREAT AUSTRALIAN BASIN

BY R. B. FLINT, G. J, AMBROSE & K. W. S. CAMPBELL

Summary

During 1977-78, 32 fossilferous Lower Devonian quartzite boulders were discovered within

Mesozoic sediments along the southwestern margin of the Great Australian Basin. Previously only

two such specimens had been discovered in South Australia though similar occurrences have been

known in New South Wales since 1898. Fossils not previously recorded in S.A. include the fish

Wuttagoonaspis, the brachiopods Howellella jaqueti and Sphaerirhynchia sp.; the bivalves

Leptodesma inflatum, Sanguinolites sp. and Praectenodonta sp.; the gastropod Strapollus culleni;

and abundant tentaculitids. Similar fossiliferous Devonian rocks are not known in situ in S.A. The

probable source area is the fossilferous Amphitheatre and Mulga Downs Groups near Cobar in

N.S.W. It is suggested that boulders were transported to S.A. during the Permian glaciation and then

reworked into Cretaceous bouldery shales and sands. All but two of the boulders are found within

conglomeratic sediments at the base of the Bulldog Shale. Theories on transport processes during

the Cretaceous ate discussed; it is concluded that conglomeratic sediments at the base of the

Bulldog Shale are reworked submarine debris-flow deposits.

FOSSILIFEROUS LOWER DEVONIAN BOULDERS IN CRETACEOUS

SEDIMENTS OF THE GREAT AUSTRALIAN BASIN

by R. 8 FuIntt, G. J, AMBRose*, & K. S. W. CAMPBELL?

Summary

Font, R. B., Amprose, GP, & Camenuia, K. 8S. W. (1980) Fossiliferous Lower Devonian

boulders in Cretaceous sediments of the Great Australian Basin, Trans, R.. Soc. §, Aust.

104(3), 57-65, 30 May, 1980,

During 1977-78, 32 fossiliferous Lower Devonian guartzite boulders were discovered

within Mesozoic sediments along the southwestern myargin of the Great Australian Basin.

Previously only two such specimens had been discovered in South Australia though similar

ocenrrences have been known in New South Wales since 1898. Fossils not previously recorded

in S.A. include the fish Wuttagoonaspis, the brachiopods Howellella jaquerl and Sphaerivhynchia

sp.; the bivalves Leptodesma inflaturn, Sanguinelites sp, and Praectenodonta sp., the gastropod

Straparallus calleni; and abundant. tentaculitidy Similar fossiliferous Devonian rocks ure not

known in site in S.A. The probable source area is the fossiliferous Amphitheatre and Mulga

Downs Groups near Cobar in N.S.W, Ii is suggested that boulders were transported lo S.A.

during the Permian glaciation and then reworked into Creiacebus bouldery shalos and sutids.

All but two of the boulders are found within conglomerutic sediments at the base of the

Bulldog Shale, Theories on transport processes during the Cretaceous are discussed; |t is

concluded that conglomeratic sediments at the base of the Bulldoy Shale are reworked sub-

marine debris-flow deposits.

Introduction

Fossiliferous Devonian quartzite boulders

from Cretaceous sediments were first de-

scribed from White Cliffs Opalfield in NSW.

by Dun (1898). P, J, Russ collected the first

fossiliferous boulder in S,A. in 1966 Tron) an

opal shaft at the Andamooka Opalfield It was

thought at the time that an opal miner may

have brought the boulder to S.A, from White

Cliffs, However, aller discovery of ja second

fossiliferous boulder near Dalhousie Springs by

M. C, Benbow, the geological implications

Were assessed by Campbell e¢ al, (1977). They

concluded that the fossiliferous boulders, like

those at White Cliffs. were derived from the

Devonian Amphitheatre Group near Cobar in

N.S.W,. and that they were transported to

S.A. during the Permian glaciation, later to be

reworked into Cretaceous steuta.

* Geological Survey of South Austraha, 191

Greenhill Rd, Purkside. S. Aust. 5063.

Department Of Geolegy, Australian National

University,

1 Carr, 8, G., Oliver, J. G,, Conor, C. H. RH. &

Scott D. C. (1978) Andamvooku Opal fields; The

gcology of the precious stones field and the re-

sult of the subsidised mining programme 5.

Aust, Dept Mines & Energy Rept 78/5 (unpub-

lished).

2 Vouk, M. F. (1978) Aspects of the geolory of

the Stuart Creek area, north of Lake Torrens,

South Australia, B.Sc. (Ions.) thesis, Univer

silty of Adelaide (unpublished).

During geological mapping of the BILLA

KALINA 1:250 000 map sheet and subsequent

investigations elsewhere along the margin of

the Great Australian Basin, a further 32 fos-

siliferous boulders were discovered, containing

many species not previously recorded in S.A.

Their occurrence and distribution permit 4

few assessment of their probable ongin and

modes of transport, ‘The earlier concept of

Campbell et al. (1977) is substantiated,

Geological setting

Stratigraphic units in the southwestern Great

Australian Basin include the Algebuckina

Sandstone, Cadna-owie Formation and Mount

Anna Sandstone Member, Bulldog Shale and

overlying younger Mesozoic sediments (Fig |).

The stratigraphic nomenclature adopted here

ix that of Wopfner ef al. (1970) based on

the Oodnadatla-William Creek area (for the

Marree area see Forbes 1966),

The following gealogical summary is com-

piled feam Wopfner & Heath (1963), Lud-

brook (1966, 1978), Wopfner et al. (1970),

Morgan (1977), Carr et al, (1978)4,) Pitt

(1978). Vouk £1978)" and from observations

during geological mapping of the BILLA

KALINA [:250.000 map sheet.

Vhe Upper Jurassic Algebuckinu Sandstone

consists of fine to medium-grained sandstones

and kaolinitic, conglumeratic sandstone, Clasts

within the conglomeratic sandstones arte chiefly

58 R. B. FLINT, G. J. AMBROSE & K.S. W. CAMPBELL

SIMPSON DESERT

=— —BOGDMADATIA —

TSILLAKALINA 1250. 000

dese” MAP. SH

rounded to well-rounded white quartz pebbles.

However, weathered acid porphyry and quart-

zite pebbles and cobbles are also common, The

unit Wes deposited m a low gradient. fluviatile

environment,

Transgceession tw the Neocomian led to ibe

disconformably overlying Cadna-owie Forma-

tion, consisting of marginal marine very fine to

Medium-peruined. micaceous and oceasionally

conglomeratic sandstones. Clasts within the

sandstunes ure chielly pebble, cobble and

boulder-sized quartzites up to 1 x J x 0.5 m

Later in the Neocomian, partial regression led

to the deposition of the coarser Mount Anta

Sandstone whieh eoasists of medium to conrse-

gmincd. feldspattue ond conglomeratic sand-

stones and micneros sandstones. Clasts of

perphyritic acid volcanics charactertse the con-

\ bARE

— fi wyre )

i ——— =,

lye id

: | camozor

ALEJEN TOAONIAN

Beck: to

CRETACEOUS

SS —s—

Lh}

3 “ a ue ma ' = 3

Ovaly, yO Colm ae am sed Kandy a

DAWA MWHE FWAA [loty = =

Hye VD (Yaya to ae 3

piualamcucihs Pru «unr eooe =

PLA RHL De Stl’ jlo pip 5

1 ere ee OC en ee Tt Et a =

= |2 |

Heed tats crt THR Ede idee taueerpt it = 2

tied Abel Ghodt — = =

= &

CHR) Soatemment cceko at or }82 2

Gorl ehe ono 4S

HORA poy Mipwatiivee cian vied meeetere e

1s , q 5

.\ TIBAR DESERT REET RES ida |

STRZELECK! DESERT |

glomeratic sandstones, though white quartz

and quurizite clasts are also common, The

clasts are sub-rounded to well-rounded and in

ihe size range 0.02-0.2 m. Concave and festoon

cross bedding are ubiquitous; forescts are up te

2m high and bedding within the foresets is

graded.

The second Cretaceous marine transgres-

sion, in Aptiaa time, was of much greater ex-

tent and resulted in marine shale deposition

(Bulldog Shale) over a large area of the Great

Australian Basin, Basal lithologies of the Bull-

dog Shale range from bouldery to conglomera-

tic sand to grey shales, cone-in-cone limestones

and sandy limestone, Fossil tree trunks are

common, Clasts within the conglomerate sedi-

ment are predominantly quartzites with minor

acid porphyries and banded chalcedony, and

FOSSILIFEROUS LOWER DEVONIAN BOULDERS 59

occur in either bioturbated grey shales or thin _ silts, and fossiliferous limestones. A subse-

coarse-grained sand lenses (Fig. 2). The sand quent regression and a further two transgres-

lenses vary from only a few centimetres thick sive-regressive cycles occurred in the Albian

to massive lenses up to a metre thick With to Turonian.

boulders scattered in the sandy matrix (Fig. The fossiliferous Devonian quartzite boulder

3). These sediments interfinger with and are from the locality southeast of Oodnadatta is

the only specimen weathered out from mar-

CcuX

oe “

yer

Shale, 60 km north of “Billa Kalina”; 3, Rounded quartzite cobbles near top of coarse-grained sand

lens, and overlying bioturbated marine shales (Bulldog Shale) from 20 km east of Billa Kalina

locality 1; 4, Well-rounded quartzite boulder lag near Billa Kalina locality 2, Many boulders are

fractured due to Holocene weathering; 5, Surface gibber lag east of Coober Pedy: cobbles and

boulders derived from basal sediments of Bulldog Shale. Clasts are dominantly quartzites; less than

1% contain Devonian fossils.

60 R. RB. FLINT, G. J. AMBROSE & K. 8. W. CAMPRELL

ginal marine sediments of the Cadna-owie For-

mation, All other fossiliferous boulders (in-

cluding the original two specimens discovered

at Dalhousie Springs and Andamooka, and

previously thought to be derived Irom the

Cadna-owie Formation) have weathered out

from basal conglomeratico sedimenis of the

Bulldog Shale,

Description of the boulders

Basal conglomeratic sediments of the Bull-

dog Shale crop out poorly but erosion has re-

sulted in Alimerous clasts from the conglo-

merates, ranging in size from pebbles to

boulders, forming a lag on the present day land

surface (Figs -4, 5), Physically-resistant clast

types dominate, mostly quartzites (feldspathic

and/or tithe), with minor porphyritic acid

volcanics and whitish-grey banded chalcedony,

Granite, gneiss, quartz and shale clasts are

rare, hut may be locally more common tear

Proterozoic oliterops.

A high proportion of the quartzite boulders

have abundant clay pellet impressions, » fea-

ture typical of the Upper Proterozoic Arcoona

Quartzite on the Stuart Shelf, The porphyritic

acid volcanics are similar to the Middle Pro-

terozoic Gawler Range Volcanics on the Gaw-

ler Craton (Wopfner et al 1970), while

banded chaleediny clasts ure similar to cherts

and siliceous Goneretions in the Cambrian An-

damooka Limestone,

Less thatt 1% of all boulders contain De-

vonian fossils, The fossiliferous boulders are

siliceous, feldspathic and lithic quartzites. They

consist of quartz-rich, medium-grained sand

(0.2-0.3 mm) and minor (<10% ) potash feld-

spar grams cemented by secondary quartz

overgrowths. The lithic quartzites contain

small Fragments of sericitic schists and ucid

porphyries (Whitehead 1978)". Tt is not pos-

sible (o distinguish |ithologically between fos-

siliferous Devonian quartzites and other

quartzite clasts.

Faunas of the boulders

In the two fossiliferous Devonian boulders

previously recorded in South Australia (Camp>

bell et al. 1977), the specimen from Dalhouste

Springs contained the brachiopod Huwellelly

jaquer’ (Dun) und bivalve Aetinepteria sp.

these were also present in the specimen col-

jected from Andamooka, In the latter sample

" Whitelreasl, S. (1978) Description of quartzite

boulders, Amde!l Rept. No. GS 415/79 Huinpub-

lished).

tentaculitids and brachiopod /yorrhiy sp. were

also present, The fossils found in the boulders

during 1977-78 are documented helow, and

intlude many species not recorded previously

in the boulders. All specimen numbers refer

to the fosstl collection of the Geological Sur-

vey of South Australia,

Billa Kalina locality | Cat.

136°08 00"B) — Specimen

29-34. 39,

Fish plate: Witlageonaspis sp. (Pig, 6)

Brachiopods: Howellella jaqueti (Dun)

Brachiopoda indet.

Bivalves; Lepiodesma inflatem (Dun)

Bivalvia indet.

Tentaculitid; Terdeulites sp. (Fig. 7)

Billa Kalina locality 2 (lat 29°28°00"S, long,

134°06'S0"E} — Specimen numbers 6139 RS

35-36.

Brachiopod: Howellella jayuet? (Dut)

Billa Kalina locality 3 (lat. 29"°58'20"S, long.

134°12'S0"E) — Specimen numbers 6138 RS

7a-T7

Brachiopoda inctet.

Bivalvia indet,

Fish plates and spines

Billa Kalina tloeality 4 Uat. 29°57'30"S, long,

136°18'35"E) — Specimen numbers 6/38 RS

‘78-85,

Brochiopods: Mowellella jaqueri (Dun)

Brachiopoda indet.

Bivalves: Sanguinolites sp,

Bivalvia indet.

Gastropods: Straparollus éullent (Dun) (Fig. 8)

Holapea sp..

Murchisoniidae indet,

Echinodermata indet,

Fish Plates and spines

Billa Kalina locality 5 (lat,

136°2)'0S°E) — Specimen

Tentaculitid: Tentaculites sp.

Crinoid ossicles

Bryozoa indet.

Billa Kalina lacality 6 (at 29°12'15"S, long,

136°09'05"E) — Specimen number 6139 RS

38.

Bivalve: Bivalve indet.

Crinoid ossicles

Billa) Kalina lecality 7 Cat. 29°02°05°S, long.

135°12'20"E) — Specimen number 5939 RS 92,

Brachiopod: Brachiopada indet.

Crinoid ossicles

Billa Kalina locality & (lat. 29°55°00"S, long.

135°49'30"E) — Specimen numbers 6038 RS

12-13,

Brachiopods: Stropheodontid (probably Mese-

douvillina or Melearnites) (Fig. 94

Brachiopoda indet,

29°28'10"S, long.

numbers 6139 RS

29") 100"S, long,

fumber 6139 RS

FOSSILIFEROUS LOWER DEVONIAN BOULDERS 61

Tentaculitid: Tentaculites sp.

Crinoid fragments

Bryozoa indet.

Moolawatana (lat. 20°52'12"S, long. 139°38’00" EB)

— Specimen numbers 6838 RS 129-132.

Brachiopods: Howellella jaqueti (Dun) (Fig.

10)

Brachiopoda indet.

Bivalves: Leptodesma inflatum (Dun)

Bivalvia indet.

Tentaculitid: Tentaculites sp.

f- .

a ees

d=? . 38

poe or

“Moolawatana” locality; 11, External mould of Sanguinolites sp. from Stuarts Creek locality, speci-

men 6337 RS 21.

62 R. B. FLINT, G. J. AMBROSE & K. S&S W. CAMPBELL

hol HRAS

PRAHD VEY

Amapedia

BASIN. fC

| DFFICER

Lrerno

Major pe

anpertet hip

Ch Ae dros els |

VICTHHIA

erlicmas

T Midi foe |) Adee Geen pnd line

Zoawls Lee = BS White

‘i

7) VASMAMN) A

D5rwn hed G Wieaeen

Loree iw Wee AlN

Fig, 12. Locality plin showing disitibution of

husins incorporating Cretaceous and Permian

sedimen(s in central and eastern Australia.

PTRMLAN oie

Vee Lopraet a lel

Codnadaiia (al. 27°55°30"S, Jong. 135"46'40"B)

— Specimen Numbers 6042 RS 92-93,

Bivalve: Praecienodanta sp,

Tertaculitid, Tevtiuentites sp.

Sivaris Creek (lat, = 3O°US45"S, long,

see se sl — Specimen numbers 6337 RS

21.34.

Brachiopods: Sphivriniyachin sp.

Howellella jaquetti (Dun)

Bivalves: Suaeuinaliters sp. (Pig. it)

Tentaculitid; Venracelies sp.

Crinoid ossicles.

Provenance of the Fossiliferous boulders

Nether the invertebrate not the vertebrate

faunas preserved in the boulders have been re-

cordet trom in situ Devonian sediments in

basins i) S.A. or the adjacent Amadeus or

Georgina Basins, The only possible Devonian

vertebrates known from §.A, are the fish seales

from a mudstone at 817-823 m io Munyarai

No. | within the Officer Basin (Pig. 12), but

these were nol positively identifiable (Gilbert-

Tomlinson 1969)4. Devonian placoderny re-

mains from the Amadeus and Georgina Basins

are bothriolepids (Young 1974) which are nat

similar to the specimens from the boulders, No

Devonian invertebrates are kiown from the

above basins, However, as has been indicated

previously, both the lithologies and inverte-

brate faunas are very similar to those from the

Amphitheatre Group near Cobar in N.S.W.,

described by Landrum (1975), and to those

from the boulders in Cretaccous sediments at

White Clilfs, N.S.W., described by Dun

(1898),

On the other hand, marine Lower Devonian

sandstones with comparable invertebrate

faunas to those at Cobar are also known (rom

the Mt Ida Formation of central Victoria and

the Elden Group of western Tasmania. These

have to be considered as alternative source

ureas, but there are good reasons for rejecting

them, The absence of Notecenchidium trom

the boulders in §,A. is taken as evidence

ugainst either a Victorian or a Tasmaniait

source because this genus js relatively common

in a hard quartzite in both these areas, The

durability of this material is attested by the

fact that Netocenchidium is among the more

common fossils in the Lower Devonian

boulders from Permian diamictites in north-

eastern Victoria. A secand important feature is

Ihe abundance of Howellella jagueti in

boulders from S.A, Although Howellella oc

curs in a variety of forms at Heathcote, ‘Talent

(1965) records that they are poorly pre-

served. ‘The genus is also poorly represented

m the Eldon Group. A. jaqueli is one of the

Most common species in boulders from S.A.,

as it is in several horizons in the Amphitheatre

(Group,

Although there are now many more boulders

with a wider range of species than was known

previously, iL sul] is possible to match the en-

tire invertebrate fauna with that from the

Amphitheatre Group, In the absenee of a

complete account of the Eldon Group fauna,

this evidence of itself can be no more than

suggestive; but taken in conjunction with the

data on Notoconchidiun and Mowellella given

above it is more persuasive of a Cobar source.

! Gilbert-Tomlinson, J. (1969) Fossils from Mun

yarai No. | Well, Officer Basin, South Australia.

‘ “Continental Of: Company of Australia Ltd.

Munyarai No. t, South Austratia,” Well com-

pletion report, S, Aust, Dept Mines & Energy

envy. 979 (unpublished),

FPOSSILIFERGUS LOWER DEVONIAN BOULDERS 63

Further weight is lent to this view by the

discovery of fossil fish fragments in boulders

at three of the Billa Kalina localities, So far

as We are aware no Devonian fish beds ure

known from Tasmania, though they are well

eaposed in central and eastern Victoria and

over much of central N.S,W., where they are

mainly of Late Devonian age, The most im-

portant discovery is the fragnreni referred to

Wuttagounasply Ritehie (1973) from the

Mulga Downs Formation of probable Middle

Devonian age in the Mt Grenfell area wesi of

Cobar, und Mt Jack north of Wileatnia, This

specimen is only an impression of a fragment

of an undetermined bone, but its ornamenta-

tion is distinctive, Its identifieadon has been

gantirmed by Ritchie.

We therefore conclude from the available

evidence that the source for the fossiliferous

boulders is in the Cobar région, the boulders

having been tfafisported at least 1000 km in

a weslerly to vorthwesterly direction.

Transport oF the boulders

A palacoenvironmental interpretation of

JurassieCretaceous sediments in the southe

western Great Australian Basin by Waoplner

et al (1970) indicates that transport of

boulders in this direction and for this distunce

during the Mesozoic Was improbable. How-

ever, Permian ice may have transported the

fossiliferous boulders from the Cobar area to

northern S.A. and the unconsolidated Per-

nian diamictites could then have heen te-

worked iuta Mesozoic sediments (Campbell er

al, 1977), Thus (wo phases of transport would

be involved,

fu northern S.A... Pormian diamictites gre

preserved in Palacozoie basing under the Great

Australian Basin fe.g. Arckaringa, Cooper and

Pedirka Basins) and in stall grubens within

the Gawler Block, These distributions suggest

that such deposits were once widespread but

thit they have been Jargely removed from up-

lifted areas.

Crowell & Frakes (1975) using the distribu-

tion of glacial Hl and Muvial sediments and

palaeveurrent analysis, postulated a larac

Permian continental lee cap over vorthwestern

NuS.W,. with glacial debris being shed east

wards and possibly westwards into the basins

of northeastern S.A, This interpretation differs

from that of Wopther (1990) who concluded

that the composition of erratics in Permian

diamictites of the AfcKartnga Basin indicated

Inval glaciation rather than a continental ice

shect, He suggested that Permian glaciev's

originated on uplaulted highland areas; glacial

Uecbris was dumped along basin margins and

then transported by mudflows alid turbidity

currents inta distal parts of the basins,

Though we prefer the views proposed by

Crowell & Frakes, if must be stressed that to

date no fnssiliferous Devonian boulders have

been discovered in Permiun cdiumietites in S.A.

ice-movement directions during the Permiat

are not known for northern §.A,, and there are

conflicting views on the Permian palacoen-

Vironment and likelihood of long-distance

Lransporl., Nevertheless, ice transport seems to

be the only feasible means for tfansporting

boulders from the Cobar area to northern

S.A.. and the Permian is the only period in

the required iuterval for which glaciation of

an Appropriate magnitude has been demo-

strated,

Final entplacement of the boulders

The processes by which the Cretaceous

boulder heds were formed have been debated

for nearly 100 yeurs, This paper is not in-

tended tw provide a detailed discussion of the

problem, but it does add another feature that

requires explanation — viz. the distant pre-

Venanee of same of the houlders. It has been

thought appropriate that 4 summary of the

issties should be presented,

Beatures requiring explanation are

(a) the scatter of boulders throuyly a sandy

or shaly matrix which is bioturbated in places;

(b) the rounded form olf most of the

boulders, though an occasional fuectted or

striated boulder has been noted (Jack 1915;

Woolnough & David 1926);

{c) the predominunee of quartzites among

ihe boulders, with avid porphyries and chal-

cedony forming the majority of the remainder;

(4) the occurrence of fossiliferous boulders

in Cretaceuus rocks from While Cliffs to Bal-

housic Springs

The shape and eooposition of the boulders

indicates (he operation of processes that have

removed all but the Most divable materials,

and thal these processes were al least in part

physical. Tumbling experiments by Abbott &

Peterson (1978) showed ehert, quartzite and

rhyolite to be the most durable rock types, fol-

lowed by metabreccia, obsidian, mietasand-

stone, gneiss, ‘gaiites’, melabasall, marble and

schist, The first three rocks are also chemically

resistant.

64 kK. B. FLINT, GJ

One possihle source for many of the clasts

is in Proterozoie/Cambrian rocks such as

those of the Gawler Craton and Broken Mill

Block which could provide abundant quart.

zite, acid porphyry (Gawler Ranye Voleanics)

and chalcedony (Andamooka Limestone). A

second source would be the Permian dhamice

tite, mentioned pbove, which is known ta con-

tin clasts of limestone, schist, gneiss, eranite,

acid porphyry, quartzite, quartz, banded iron

formation, chert and shale, The original source

of many of these clasts must have been the

Profterozoic/Cambrian rocks indicated above.

Both the above sourges would have been sub-

jected ty prolonged Weathering between the

Permian and the Early Cretaceous, and trans-

port to the Cretaceous sea with subsequent

shoreline deposition would have resulted in

the removal of the less durable clasts,

Brown (1905), Jack (1915), Woolnough &

David (1926) and Vnuk® considered that ice

rafting was responsible for the final transport

of the boulders and that they were muinly

dropstones. [n our yiew this mechanism ts nae

acceptable. If the proposed ice was culved off

from glaciers there would be oo explanation

for the dominance of resistant clasts, their

rounded shapes, or their abundanee ever su

large w geographical distribution, If sea ie

picking up clasts from 4 boulder-strewn

shore were proposed, it would be possible ta

explain the clast types and shapes, but the prob-

blems of volume and distribution would re-

main. In addition there is no independent evi-

dence of glacial conditions in the Early Cre-

taceous, though the area in question would

have been within 30° of the pole,

Woolnough & David (1926) also con-

sidered, but rejected, tree rafting as a possihle

transport mechanism for the boulders. Much

later Wopfner et af, (1970) reinstated the pro-

posal because of the abundance of fossil

woul in Early Cretaceous sedirients, However

AMBROSE & kK, 8, W. CAMPBELL

because of the abundance and concentration

of boulders within particular horizons, tree rafl-

ing was not accepted as the sole transport

mechanism, Since they considered the boulder

beds to be restricted to margins of basement

highs, they also proposed that the boulders

originales on shorelines and migrated down-

slope by slow sediment creep, [t is this latter

Suggestion that seems to us to provide a clue

io a possible solutiwn — namely that they are

reworked debris-flow deposits, Bouldery de-

bris-flow deposits typically consist of a massive

fine-grained matrix with randomly dispersed

boulders [Fisher 1971; Middleton & Hampton

(973; Carter 1975; Hampton 1975) but the

beds under discussion are not of this type,

Some other processes must have been opera-

tive in addition, We propose, therefore, that

boulders. cobbles and sand were transported

basinwards trom a boulder-strewn shore ling

in a clay-rich, watery matrix over low angle

slopes. The debris flows were episodic events,

permitting time for some reworking of the

debris-flow sediments, and subsequent shale

sedimentation and bioturbation. Winnowing of

muds and fine sands from the debris-flow seci>

ments by currents, and possibly by waves. has

resulted in some of the boulders and cobbles

being concentrated in thin, course-grained sand

lenses, Complete winnowing of the fines and

further shale deposition has resulied in same

boulders being located within bioturbated

shales,

Acknowledgments

Apprecianion is extended ta G, Johansen

(Newmont Pry Led), M. FP Vnuk (Adelaide

Lyiversity) and M, C. Benhow. R, A, Callen

and S. Ro Hewles (Geological Survey of South

Australia) who collected some of the fossili-

ferwus boulders and kindly made then avail-

able for cXamination,

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of abrasion durability on conglamerate clust

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Camprers, KS. Wi, Roceas, P. A. & Brapow,

M. C. (10977) Bossiliferaus Lower Devonian

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9-13.

Carrer, ROM. (1975) A discussion ane chissifi-

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249. Elsevier.

MippLeTon, G. V. & Hampton, M. A. (1973)

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(Chairmen) “Turbidites and deep water sedi-

mentation.” Short course lecture notes; pp. 1-38

(Soc. econ, Paleont. Miner.: Los Angeles).

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An Unusual Arthrodire from the Devonian of

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WooLnouanH, W. G. & Davin, T. W. E. (1926)

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Basin, South Australia. In “Second Gondwana

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Jurassic-Cretaceous rocks of western Great

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& Heatu, G. R. (1963) New observations on

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PROGAMOTAENIA NYBELIN (CESTODA: ANOPLOCEPHALIDAE): NEW

SPECIES, REDESCRIPTIONS AND NEW HOST RECORDS

BY I, BEVERIDGE

Summary

The following species are described: Progamotaenia spearei sp. nov., from Thylogale stigmatica,

distinguished by its small size, in having paired uteri, a fringed veleum and testes in two groups,

and Progamotaenia johnsoni sp. nov. from Lagorchestis conspicillatus, which has an external

seminal vesicle covered with glandular cells and testes distributed in two elongate groups. P.

bancrofti (Johnston) and P. diaphana (Zschokke) are redescribed, and Lasiorhinus latifrons is

considered to be the usual host of the latter species. P. zschokkei (Janicki) is reported for the first

time from Macropus agilus, Onychogalea fraenata and O. unguifera; additional records of this

species from Petrogale penicillata, Lagorchestes conspicillatus and Thylogale stigmatica are given.

PROGAMOTAENIA NYBELIN (CESTODA:

NEW SPECIES, REDESCRIPTIONS AND

ANOPLOCEPHALIDAE):

NEW HOST RECORDS

by L Beveripce*

Summary

Bevermnce, L (1980) Progamataenia Mybelin (Cestada: Anoplocephalidac): new species,

tedescriptions and new host records. Trans. R, Soc, S. Aus, 104(4), 67-79, 30 May, 1980.

The following species are described: Progamotaenia spearei sp. nov., from Thylogale

stigmatica, distinguished by its small size, in having palted uferil, a fringed velum and testes

in rwo groups, and Progamotaenia johaseni sp. nov. from Lavorchestis conspicillares, which

has an external seminal vesicle covered with glandular cells and testes distributed in two

elongate groups. P. barcrojti (Johneton) and P. diaphana (Zschokke) are tedescribed, and

Lasiorhinus latifrous is considered to be the asual host of the batter species. P_ zschokkei

(Janicki) is reported {or the first time from Macropus agilis, Onyehogalea fraenata and

O, wiguifera; additional records of this species from Petrogale peniciliaia, Lagorchestes con-

spicillatus and Thylogale stigmatica are given.

Introduction

Although the anoplocephalid ecstodes of

Australian marsupials have been the subject of

a recent review (Beveridge (976), continued

collecting has resulted in the discovery of ad-

ditional new species of Progamotaenia (Bever-

idge 1978, Beveridge & Thompson 1979), To

date most collections have been from miar-

supial species inhabiting the south-castern part

of the continent. Recent collecting from mac-

Topodids in north Queensland bas led te the

discovery of two new species of Pragamo-

taenica.

Progamotaenta banerofti and P. diaphana,

were recently redeseribed by Beveridge (1976)

on the basis of very limited or poorly preserved

material only. Both are well represented in

recent Collections, and the opportunity is taken

here to describe them fully,

Materials and methods

Cestodes collected from the small intestines

of macropodids were washed in tap water, re-

laxed in water for several hours and fixed in

10% formalit or Serra's fluid. They were

staimed with Celestine blue, cleared in methyl

salicylate or clove oil and mounted in balsam.

Wand cut transverse sections and serial histo-

logical sections cut in transverse and longi-

tudinal planes were prepared, Drawings were

made with the aid of a cameta lucida, Mea-

surements. are given in mm as the range fol-

lowed by the mean of five measurements

(where available) in parenthesis,

Type specimens have been deposited in the

South Australian Museum (SAM).

* [Institute of Medical & Veterinary Science,

Frome Rd, Adelaide, S. Aust. 5000,

Progamolaenia spearei sp, nov.

FIGS i-8

Types: holotype (slide) from small intestine

of Thylogale stigineitea Gould 1860, Tolga

Queensland, 16 x, 1978, collected by I,

Beveridge, in SAM V1920; 4 pavatype slides,

same data VIG2I-V1924: 1 paratype, spirit

material and serial sections VL925, V1926.

Description; Length 26-30 (28); width 5-7

(6): seolex diameter 131-152 (1.44): sucker

diameter 0.56-0.74 (0.67) x 0.47-0.58 (0.55);

neck 0-0,21 (0,09); no. proglottides 71-85

(78); mature proglottides 3.84.0 (3.9) x

0.21-0.28 (0.23); gravid proglottides 4.1-5.8

{5.4) x 0,56—0.74 (0.65): cirrus sac in mature

proglottides 0.60-0.92 (0,81) & 0.084112

(0.10); cirrus sac in gravid proglottides 0,93-

0.98 (0.94) x 0.11-0.14 (0.12); no, testes per

proglottis 30-40 (34); testis diameter 0.06—

0,09 (0.08); ovary 0.50-0,456 (0.53) x 0.18-

O21 (0.20); vitellarium O.11-0,18 (0.15) x

0.08-0.12 (0.10); dorsal osmoregula-

tory canal 0,02-0.03 (0.021; ventral osmoregu-

latory canal 0,03-0,09 (0.07); cgz 0.06-0.08

(0.07); pyriform apparatus 0,03-0,04 (0.04);

oncosphere 0,02,

Short broad tapeworms with relatively few

proglottides, Scolex squat, almost globose,

prominently four-lobed, each lobe with muscu-

far, cup shaped sucker. Neck absent or, if pre-

sent, very short, segmentation beginning very

close to suckers, Proglottides extended trans-

versely, craspedote with broad, fringed velum

consisting of about 25-35 tongue shaped pro-

Jeclions which are frequently felded and over-

hand 1/2=2/3 of the adjacent proglottis-

Mature proglottides with approximate length:

68 I, BEVERIDGE

Figs 1-8. Progamotaenia spearei sp. nov. 1, scolex; 2. transverse histological section through cortex

showing musculature; 3. egg; 4. mature proglottis; 5. gravid proglottis; 6, cirrus sac; 7, lateral re-

gion of mature proglottis prior to vaginal atrophy and uterine filling; 8, lateral region of mature pro-

glottis at commencement of uterine filling, showing atrophy of vagina. Scale lines 0.1 mm.

SPECIES OF PROGAMOTAENIA (CESTODA: ANGPLOCEPHALIDAB) 69

width ratio of 1:14 to 1:20. Gravid proglot-

tides with ratio 1;6 to 1:10, Cortex thick,

longitudinal muscles developed, numerous, rot

alranged in regular bundles, denser towsirds

cortico-medullary junction, Tratsvetse muscles

well developed, forming thick band runing

along cortico-medullary junction, Dorso-ven-

tral muscles prominent, crossing cortex and

medulla at irregular intervals. Longitudinal

osmoregulatory canals paired, Ventral canal

wider than dorsal canal, situuted medial to it.

Two transverse canals connect left and right

osmoregulatory canals at posterior fnarsin of

each proglottis, Canal connecting ventral ves-

sels of moderate size, readily observed: canal

connecting dorsal canals extremely fie, seen

only with difficulty, Fine accessory canals as-

sociated with ventral canal in some proglot-

tides; accessory canals branch and anastomose

imegularly, Junction of osmoregulatory canals

in seolex not seen. Genital ducts cross osmo-

regulatory canals dorsally, Genital atrium

prominent, very long; walls lined with

thickened tegument, opening in middle of

lateral proglottis margin. Cirrus sac clongste,

musculature of walls strangly developed, cross-

ing beyond osmoregulatery canals. reaching

almost to ovary. Cirrus narrow, distal ‘third

covered wilh numerous prominent spines: mid.

third unarmed, greatly coded when retracted.

vncoiled when cirrus is everted, Internal se-

minal Vesicle prominent, elongate, External

seminal vesicle absent, Vas deferens coils an-

teriorly and medially from cirrus sac. Wasa

efferentia nol seen, Testes distributed in two

compact clusters anterior Un cirrus sac. extend

ing medially from osmoregulatory canals to

poral side of ovary; never extending medially

hevond ovary to form single band. Vayina

tube-Jike, opening to genital atrium posterior

lo cirrus sac. Vagina leads medially lo dimmu-

tive, ovaid, seminal reeepticle situated pos-

terior to median pole of cirrus soe, lateral to

ovary, Ovary fan-shaped, composed of

numerous clavate lobules, on ventral aspect of

mednlla, Vitellarium ovotd, situated posterior

and dorsal to ovary Mehtis’ gland spherical,

medial to vitellarium, Uterus transverse, tube-

like, paired in cach proglottis, anterior to

ovary, Fully developed wferus sacciform with

prominent anterior diverieulay posterlor diver-

ticula very small, Uteri fill space hetween

osmoregulatory canals but do not extend be-

yond canals except in Jast few gravid: progtot-

tides: uteri croxs canals dorsally but da nat

reach posterolateral corners of proglottis, Egg

spherical, thick-shelled. Pyriforny apparatus

conical, terminating in reflexed filaments.

Genital primordia appear In &-10th progh-

tls; genital organs are developed by 15-18th

proglottis: sperm present in internal seminal

vesicle in |5—20th proglottis; (line of seminal

receptacle and alrophy of vagina oceur in 146-

24th provlottis; uterus begins to All in 22—-26th

proglottis, eggs fully formed in 69-73nl pro-

glottis,

Vestigial supernumerary vitellaria, ovaries

or uterine fragments present in proglollides of

some strobilac, of variahle size, arranged be-

Iween Iwo normal sets of genital organs.

Discussion: Pragamolarnia spearei most

closely sesernbles FP, prateregyna (Fubrmann

1932) [tm external features, being a small

worn, with few proglotlides and with a fringed

velum. It differs in the shape of Fringes of the

vellim, the occurrence of testes in two distinet

groups rather than in a continuous band and

in the oecurrenee of vaginal alrophy following

insemination. P eynandroliwariy Beveridge &

Thampson 1974 is another small species, bul

the velum is nol fringed. Po speare? resembles

Po fagorchestis (Lewis 1914) and P. thylogale

Beveridge & Thompson 1979 in having a

fringed velum, paired uteri and testes occurring

in two lateral groups, but differs fram both

species in ils small size, small number of pro-

glattides, the rupidity af development of the

genital organs in the strobila and the small

number of testes.

This species is named after Or R. Speare,

James Cook University of North Queensland,

in appreciation of help given in collecting

material,

Progamotaenia johnseni sp. nov.

HIGS 9-15

Jypess holotype (without seolee) from small

infesting Of Lagerchevtes conspicihitie Gould,

(442, Mingela, Qneensland, 1 4. 1979, col

lected by |. Beveridge. 4 slides, spirit material

aml serial section in SAM V1918; paratype

slide, sane data, VIGTY,

Matevial examined: from Lagerchestes can-

yiicillatas: types; 4 specimens Cuou pray),

Trkemman Station, Olu, Tis d977, BM. tol.

son.

Deseriptions Length (78 Cholotyped; walth 13

(holotype): scolex diameter O74-1.01 (MN RA47

sucker diameter 0,30-40.42 (0.92) ~ O.28-0.36

70 I. BEVERIDGE

eseaien

rrr pitta

qs,2 2

PO. alin

SPECIES OF PROGAMOTAENIA (CESTODA: ANOPLOCEPHALIDAE) TL

(0,31); neck 016-0,36 (0.26); no. proglot-

tides 272 (holotype); mature proglotlides 5,4—

7.0 (6.2) x 0,52-0.56 (0,54); gravid proglot-

tides 9.4-9.8 (9.6) x 0.92-0,99 (0.96): cirrus

sac in mature proglottides 046-1,31 (0.90) %

0.16-0,29 (0.25): in gravid proglotiides 118—

1,18 (£149) x 035440,36 (0.95); no. testes per

proglottis 100-190 (178): testis chameter 0,05—

0,08 (0.06), ovary 0.624180 (0-72) x O44—

O98 (0.36); vitellanitim 0.30040 (O37) &

0.17-0.23 (M18): Meblis’ gland 0,10-1,14

(0.12): dorsul osmoregulatory canal 0.02—-11.04

((\.03); ventral osmoregulatory canal 0,08-

0.29 {O.18i2 egg 0.064-0,072 (0,068); pyr-

form apparatus O0.024-028 (0.025); anca-

sphere O.00960,U16 (0.015),

Laree, broad, ribhon-like worms. Scolex

broad, four-lobed, with cup-shaped sucker al

apex of each lobe, Suckers with anterior inar-

gins cleft, Neck short, Proglotlides greatly ex-

tended transversely, eraspedote, with broad,

fleshy, folded velum covering much of adjacent

proglottis. Mature proglottides with approxi-

mite length:width ratio of 1:10 to ts13. Gra-

vid proglottides with ratio of 1:9 to Is1)-

Longitudinal musculature powerfully — de-

veloped, composed of patlisades of muscle

bundles. Bundles circular or oval in seccian:

ouler biindles smaller, with fewer fibres. Outer

lonoitudinal musculature consists of rng of

individual fibres, inymediately external to

muscle bundles, Transverse muscles well de-

veloped, furminy broad band immediately m-

ternal to lonwitudinal muscle bundles. Few,

scallered transverse muscle fibres present in

ouler cortex. Towards lateral margins ol pro-

slottides, trinsverse muscles from cortex and

cortica-medullary junction fuse into thick band

of muscle encireling cirrus sac and extending

tO genital atrium, Dorso-ventral muscle fibres

well developed, promment, crossing cortex and

medulla at regular Iotervals. Longitadinal nos-

morevulatory canals pulred, Ventral canal

wider than dorsal canal, situated medial to it,

Transverse canal connects left and right ven-

tral canals at posterior margin of cach praglor-

fis. Scolex osmoregulatory canals not seen,

Genital duets cross osmoregulatory canals dor-

sally, Genital atrium shallow, with corrugated

walls, Opening in middle of lateral proglottis

margin. Cirrus sac powerlully developed, wilh

thick muscular walls, extending (o medial mtar-

gin of, of beyond longitudirial osmoregulatery

canals into medulla. Cirrus wide at distal ex-

tremity, heavily armed with spines; mid-region

of narrower diameter, distal part armed, praxi-

mul part unarmed. Internal semimal vesicle

ovoid, with thick, muscular walls. Exteraal

seminal vesicle large, elongate, sometimes

coiled, covered externally with layers of glan-

dular cells, Vas deferens leads medially from

external seminal Vesicle, gradually diminishing

in diameter, Vasa elYereutia not seen. Testes

in two lateral groups anterior to female geni-

falia, each group extending from osmoregula-

tory canals medially beyood medial border of

ovary, accasionally almost to middle of pro-

glottis. Testes in 2-4 longitudinal and 1-3

transverse rows. Vagina tube-like, narrow,

opening to genital atriunt posterior to cirrus

sac, Vagine leads medially, along posterior

border of cirrus suc to ovoid seminal Tecep-

tacle situated lateral to vitellarium. Ovary fan-

shaped, composed of numerous clavate lobules,

on ventral aspect of medulla Vitellarium ovoid

to reniform, dorsal and pasterjor to ovary.

Mchlis’ gland spherical. anterior to Vitellarturn,

Uterus transverse, tube-like, paired in cach

proglottis, dorsal to ovary, Tubular uterus ex-

tends from near centre of proglottis, dorsal ta

ovary, anterior to vitellarium, terminating be-

tween proximal pole of external seminal vesicle

and seminal receptacle, Fully developed uterus

sacciform, with prominent anterivr and pos-

terior diverticula. Uteri crass longitudinal

osmoregulatory canals dorsally, extending to

postero-lateral corners of proglottis. Egg eflip-

saidal, thick shelled, Pyriform apparatus coni-

cal, terminating in reflexed filaments. Genital

primordia appear in «20th proglottis; cirrus

suo developed by 26-30th proglottis; internal

seminal vesicle fills with sperm in 33-47th

Proglottis; insemination oocurs in 40-4461

Proglotiis; Vaginal atrophy not seen; full

maturity of female genitalia reached ip c.SOth

progiottis.

DPiveussiont Although described trom a limited

amount of material, Pragamotaenia Johnson

is sufficiently distinctive to he readily recog-

nised, The gravid holotype is, unfortunately,

Pies 9-15, Pragamotaena folrasoni sp. nov. 9, scolex; 10, eve; 11, mature proglottis; 12, lateral region

of mulure proglollis showing genitalia; 13. transverse histological seetion through lateral region of

mature progtottis showing cirrus sac and muscolature, 14, transverse histological scetion through eor-

tex showing musculature; 15, gravid proglottis, Scale lines, fig. (0, 0.01 mom, figs 9, 11-15, 0 mm.

72 I, BEVERIDGE

without scolex, but the remaining specimens

are not gravid. Mature proglottides of the

specimens from Inkerman are identical mor-

phologically with those of the holotype, and

there is no doubt that they are conspecific.

There is no possibility of confusion with con-

geners that occur in L. conspicillatus, reviewed

by Beveridge & Thompson (1979), since other

intestinal species occurring in this host in east-

ern Australia have markedly fimbriated vela

(Beveridge 1976).

P. johnsoni most closely resembles P. ban-

crofti in being a very large, thick species with

greatly extended proglottides, a broad un-

fringed velum, a powerfully developed cirrus

sac and armed cirrus and an external seminal

vesicle covered with glandular cells. The last

characteristic distinguishes P. johnsoni and P.

bancrofti from all congeners. P. johnsoni is

distinguished from P. bancrofti by a smaller

scolex, a muscular wall to the internal seminal

receptacle, the presence of a pyriform appara-

tus in the egg, and most importantly of all, in

the distribution of the testes, which in P. john-

soni extend from the osmoregulatory canals

beyond the medial margin of the ovary almost

to the centre of the proglottis, but which are

restricted in P. bancrofti to the region lateral

to the ovary. Although in every proglottis of

P. johnsoni examined, the testes were distri-

buted in two groups, in some cases, the dis-

tance between the two groups of testes in the

centre of the proglottis was quite small and

examination of further specimens may well re-

veal instances in which the two groups of

testes fuse in the midline.

An unusual feature of the anatomy of P.

johnsoni is the condensation of muscle fibres

to form a sphincter-like annulus around the

distal extremity of the cirrus sac. A sphincter

surrounding the genital atrium has been des-

cribed in a number of species of Progamo-

taenia (Baer 1927, Lewis 1914), but Beveridge

(1976) considered that the structures reported

by the earlier writers in no way constituted a

sphincter, consisting as they did of an accu-

mulation of parenchymatous elements. The

structure described above in P. johnsoni is a

distinctive muscular structure which is in some

respects sphincter-like. However, its function

is not known at present.

The species is named after Mr P. M. John-

son, National Parks and Wildlife Service, Pal-

larenda, Queensland, in appreciation of help

given in collecting specimens.

Progamotaenia bancrofti (Johnston, 1912)

FIGS 16-23

Material examined: from Onychogalea frae-

nata: 2 specimens, Dingo, Qld, 12.vii.1975,

J. E. Nelson; 1 specimen, Dingo, Qld., (cap-

tive animal) March, 1978, I. Beveridge.

From Onychogalea unguifera: 6 specimens,

Wernadinga Station via Burketown, Qld,

6.viii.1979, R. Speare and P. M. Johnson; 8

specimens, Chadshunt Station via Mt Surprise,

Qld, 7.vili.1979, R. Speare and P. M. John-

son; 2 specimens, ‘Kimberley Ranges’, W.A.,

31.viii.1976, L. Keller.

Description: Length 198-312 (243); width 9-

18 (14); scolex diameter 2.21-2.75 (2.46);

sucker diameter 1.05-1.38 (1.25) x 0.88-1.28

(1.02); no. proglottides 643-672 (660); mature

proglottides 6.6-9.5 (7.9) x 0.34—0.42 (0.38);

gravid proglottides 9.2-10.6 (9.8) x 0.40-0.70

(0.55); cirrus sac in mature proglottides 0.66—

1.52 (1.11) x 0.23-0.34 (0.26); cirrus sac in

gravid proglottides 1.4-1.9 (1.6) x 0.26-0.32

(0.29); no. testes per proglottis c. 200; testis

diameter 0.06-0.09 (0.07); ovary 0.60-0.80

(0,67) x 0.24-0.35 (0.29); vitellarium 0.40-

0.57 (0.47) x 0.14-0.24 (0.18); Mehlis’ gland

0.11—0.17 (0.14); dorsal osmoregulatory canal

0,02-0.06 (0.04); ventral osmoregulatory

canal 0.22-0.35 (0.30); egg 0.036-0.041

(0.039); embryophore 0.017—0.024 (0.018);

oncosphere 0.014—0.020 (0.016).

Large, broad, ribbon like worms, Scolex

large, globular, distinctly demarcated from

scolex. Four cup-shaped suckers embedded

within scolex. Neck absent. Proglottides

greatly extended transversely, craspedote, with

broad, fleshy, folded velum radiating outwards

from strobila, covering + to # of the adjacent

proglottis. Mature proglottides with approxi-

mate length: width ratio of 1:20 to 1:23. Gra-

vid proglottides with ratio 1:16 to 1:20, Ter-

minal proglottides narrower with ratio 1:8.

Figs 16-23. Progamotaenia bancrofti (Johnston). 16. scolex; 17. transverse histological section through

cortex showing musculature; 18, 19. eggs showing variation in shape and in thickness of embryo-

phore; 20. lateral region of mature proglottis; 21. female genital complex, from hand cut trans-

verse section; ventral towards top of page; 22. postmature proglottis showing tubular uterus; 23. gra-

vid proglottis. Scale lines, figs 16, 23, 1.0 mm, figs 18, 19, 0.01 mm, figs 17, 20-22, 0.1 mm.

SPECIES OF PROGAMOTAENIA (CESTODA: ANOPLOCEPHALIDAE)

74 L BEVERIDGE

Longitudinal musculature powerfully de-

veloped, composed of pallisades of muscle

bundles. Bundles elongate, arranged radially.

bundles towards periphery smaller, with fewer

fibres, Transverse muscles well developed,

forming a Uccse band along vortico-medullary

junction, Derso-ventral fibres prominent,

crossing corles anid medulla at regular inter:

vals. Longitndinal osmoreguiatary carnals

paired, Ventral canal wider than dorsul canal,

sitvialed medial to at Small accessory canal

associated with ventral canal, on ventral side

of ventral canal, Transverse canal ¢annects

left and nigh! ventral canals al posterior mat-

gin of cach proglottis, Contplex of very

fine branching and anastomosing vessels asst

ciated with dorsal system at posterior mrareins

of proglottides. In scolex, vessels Ivad to con-

necting Ting Yessel in transverse plane at level

of anterior margins of suckers. Genital duets

cross osmoregulatory canals dorsally, Genital

atrium shallow, with corrugated walls, open-

ing in middle of lateral proglottis margin, cutes-

ing interruption af velum. Cirrus suc power-

fully developed with thick muscular walls, ex.

tends beyond osmoregulatory vessels mite

medulla, Cirrus widest at distal extremity,

heavily armed with spines; mid-region coiled,

unarmed, Internal seminal vesicle present,

usuully reflexed distally when filled. External

seminal vesicle large, cloneate, covered exter-

nally with layers of glandular cells, Vas ce

ferens inconspicuous, coils anteriorly tu testes.

Vasa efferentia pot seen, Testes distributed in

two compact groups anterior to cirrus sac, ex-

tending from longitudinal osmuregulatory

canals to lateral margin of OVary. Testes in 3-5

longitudinal and 4-6 transverse rows. Number

of testes in cach group could not be counted

accurately,

Vagina tube-like opening to genital atrium

posterior to cirrus sac, distal Vagina seen only

in serial sections. Vagina lends medially along

ventral aspect of cirrus sac, crosses tu dorsal

aspect of medulla, gradually imereasing i

diameter, Seminal reeeptacle not clearly

separated from yayina. situaled lateral to

vitellarium. Qvary fan shaped, composed of

numerous clavite lobules, on ventral aspeet of

medulla, Vitellarium reniform, dorsal and pos-

terior in ovary, partially enclosing Melis!

wland, which is spherical, anterior to vitel-

larium,

Uterus transverse, tube-like, piited in wich

proglotiis, dorsal to oVaty, Tubular Uterlis ex-

tends from near proglottis midhine, anterior to

Vitellarium and dorsal to ovary, runs along

Ventral aspect of medulla almost to longitu-

dina! osmoregulatery cunaly, Fully developed

uterus sacciform. With prominent «anterior

diverticula, and fewer, smaller posterior

diverticula; crossing longitudinal osmoregula-

tory canals dorsally, extending to postero-

lateral corners of proglottides, Egg elongate

ovoid, outer wall thin. Pyriform apparatus

absent, even in egas from faeces; embryophore

surrounding egg thick, ellipsoidal.

First mature proglottis 165-235rh; filling of

seminal receptacle occurs ut approximately

same time as sperm appears in internal seminal

vesicle; vagina does not atrophy Following in-

semination; ulerine filling commences inc.

Oth proglottis.

Discussion: The descriptions of Progamotaenia

hancrofti by Johnstan (1912), Nybelin (1917)

and Beveridge (1976), are unsatisfactory be-

cause only a limtled number of specimens was

available, The original desetiption by John:

ston (1912) was based on a single non-gravid

specimen from Onvechogalea fraenata, the

description by Nybelin (1917) was based on

four specimens from O. ungul/era, ull of which

were severely contracted, and only one was

gravid, Beveridge (1976) re-examined all these

specimens but was able to add little. The type

host, O. fraenata is now almost extinct, so that

the main source of material for the present re-

description came from the related wallaby. OQ.

lingnifera.

Although ample material was available, the

species is catremely difficult to examine be-

cause of its large size and the thickness of the

longitudinal musculature and velum, Nevers

theless, the present re-deseription supports

earlier descriptions in most respects, dilfcring

only in the features of the uterus panel external

seminal Vesicle, The utertis conimences de-

velopment as i transverse tube, gradually en-

jarginy iv disineter as it fills with cags. la post-

mature proglottides, in which the ovary las

involuted, the Uterus remains tuhe-like, with

Hitle evidence ef anterior allel posterior diver-

cua. ‘The lattur develop subsequently in gra-

vid proglottides. The lack of diverticula on the

Wteri of the holotype deseribed by Beveridge

(1976), presumably reflects the lnpmaturity of

the specimen rather than a significant

difference beiween wv and Lie new material.

A prostate ait the pragimal pole of the cirrus

sue Was dleaerlbed in 2 banevoffl by Nybelin

(1917) and Beveridge (1976). The structure

SPECTES OF PROGAMOTAENIA (CESTODA; ANOPLOCEPHALIDAE) 75

is in fact an external seminal vesicle, diflermg

from comparable structures in congeners in

being elongate rather than ovoid, and sur-

rounded by a mass of glandular cells. This

lattwr feature serves to sepurate PL henere/ti

from all] congeners except P, Jolinsant, How-

ever, here the term “prostate” has been dis-

carded in favour of “external seminal vesicle”

to avoid confusion with a structure (also

termed the prostate) described in certain spe-

cies of ihe anoplavephalid genera Anirva

Railliet 1893 and Ptandrya Darrah 1930,

Rausch (1976) has cast considerable doubi on

the existence of 9 prostate in these genera, sug-

gesting that the orga in question jis the exter-

nal seminal vesiele.

Nybelin (1917) stated that a pyriform ap-

paratus was not present, bot Beveridge (1976)

cautioned that the few specimens available te

Nyhelin may not have heen fully gravid, In

the new material, a pyriform apparatus was

found neither in the terfninal proglottides of

strobilae which were fully gravid, nor in shed

Progloetides collected From the large itestine

of the host. Tt was fot established whether a

pyriform apparatus develops in the external

environment following voiding. The anly can-

gener in which a pyriform apparatus is lack-

ing 1s P. lapgorchestis. In both species the ege

is clonpate rather than spherical ar ovoid,

Serial lonwitudinal sections of the strohila

revealed that the distal vagina is an extremely

narrow duct bul that i remains patent even

m proglotiides in which the uterts is in the

process of filling, The distal vagina was not

s¢en om every proglottis, but in a sulficren!

number bo indicate that earlier descripiions

have been incorrect, and what the distal vagina

is merely dilicull to find, even in sections,

rather than buving atrophied following insem-

ination.

Further collecting has confirmed Onveto-

valea fraenata ind O, wmeniferad as hosts of P,

banerefti, The species has not heen fhynd in

Wallabla bicoler or Serouly braelevis apart

from a single report by Sandars (1957). Her

brief descriptions do nor conform to eutlicr

more detailed descriptions {Beveridge 1976).

The location of Sandars’ specimens is \n-

known, and. their identifications may be i

error.

P, bancrofti was present in seven ot ten €,

unoulferd, with either mine or two cestodes per

wallaby. The cestodes veeutred tu the ileurn.

Progamotaenia diaghana (Zschokke, 1907)

FIGS 24-29

Material examined: types from Lasiorhinus

laiifeons; numerous fragmented specimens,

from bile duets, Swan Reach, 8.A,, 12.v,1977,

I, Beveridge; 14.1%.1978, M, Gaughwin,

Deseription: Leugth up to 102; width to 2;

scolex diameter 0,32-0,46 (0.38); sucker dia-

meter 013-0.16 (O15); neck 0,07-0.16

(O.13)5 mature proglottides 1-1-1.9 (1.5) x

0.23-0,43 (0.31); gravid proglottides 1,7-2.6

(2.0) x 0.28-0.35 (0,34); cirrus sac in matute

proglottides 917-039 (0.29) x 0.06-0.09

(0.07); cirrus sac in gravid proglotlides 0.22-

0.33 (0.28) * U.04-0,09 (0,07); no. testes per

proglottis S$9-64 (S51); testis diameter (.04—

0.05 (0.04); ovary 0,080.14 (11) x 0,04-

0.10 (0,08); vitellarium 0.06-0,08 (0,07) x

O.04-0.06 (0.05); Mehlis’ gland 0.04~0.05

(0.05); dorsal osmoregulatory canal 0.01

0.02 (0,02), ventral osmoregulatory canal

0.02-0.04 (0.03): egg 0.07-0.08 (0.08); pyri-

form apparatus 0.04-0.05; oncosphere 0,03,

Small, fragile worms, almost transparent and

casily broken when fresh, Scolex prominently

four lobed, with each muscular, cup shaped

sucker borne on arm like extentions of scolex,

Seolex frequently, but not invariably dark,

pigmented, Pigment distributed mainly on

arms and at apex of scolex. as masses of small,

brown staining accumulations of granules in

the cortex immediately below the tegument,

Small pigmented granules seatlered around

vieinily of central nervous system. Neck pre-

sent in relaxed specimens. Proglottides ex-

tensed transversely, craspedote, with narrow

fc. 0.05) straight-edyed velum overhanging ad-

jacent proglottis, Mature proglottides With ap-

proximate length: width ratia of 172.5 to 1:8,

Gravid progloitides with ratio 1:55 to 1:75.

Longitudinal muscles poorly developed, com-

posed of 2 pings of fibre butdles with 2 to 8

fibves per bundle. Tyansverse muscle consists

ef individual fibres running along cortico-

medullary jinection, Darso-ventral muscle

filwes sinvle, crossing cortex god medylla at

irregular intervals.

Longitudinal osmoregulatory canals paired,

Ventral canal wider than dorsal canal, situated

medial ti it, Two transverse canals connect

Jeft and right osmoregulatory canals at pos-

terior margin of each proglottis, Canal cone

necting ventral vessels of moderate size,

readily observed: canal connecting dorsal ves-

sels minute, seen only with difficulty, function

SPECIES OF PROGAMOTAENIA (CESTODA: ANOPLOCEPHALIDAB) 7

of osmoregulatory canals in scolex not seen.

Genital ducts cross Osmoregulatory canals dor-

sally. Genital atrium of insignificant size,

sometimes situated on small genital papilla,

Atrium in posterior part of lateral proglottis

margin, dividing margin in ratio of 1:2 to 1-3.

Cirrus sac narrow, clavate, musculature of

walls Weakly developed, always reaching ald

usually extending beyond longitudinal os-

moregulatory canals. Cirrus narrow, uncoiled,

armed with minute spines, only clearly visible

on exerted cirri. Prominent internal seminal

vesicle present. External seminal vesicle large,

ovoid, extending to Jeteral margin of, or oc-

casionally anferior to, serninal receptacle, Vas

deferens coiled, passes anteriorly, diminishing

in diameter. Vasa efferentia not seen, Testes

distributed between lateral osmoregulatory

canals anterior to female genitalia, Testes

either in two groups extending from longitu-

dinal canals to medial side of female geni-

talia, or in continuous band across proglottis,

with testes more numerous in lateral parts of

band. Both forms of testis arrangement occur

together in some strobilac, Vagina tube-like,

opening to genital atrimm posterior to cirrus

sac. Vagina leads medially to large ovoid, thin-

walled seminal receptacle. Ovary fan-shaped,

composed of numerous, clavate lobules, on

ventral aspect of medulla. Vitellarium ovoid

or reniform, posterior and dorsal to ovary,

Mchlis’ gland spherical, anterior to Vitellarium,

dorsal to ovary, Uterus transverse, tube-like,

paired in each proglottis, anterior to seminal

receptacle and ovary. Fully developed uterus

sacciform, without diverticula, crossing longi-

tudinal osmoregulatory canals dorsally and

reaching postero-lateral corner of proglottis,

Uteri of proglottis may fuse Jn mid-line on

rare oceasions. Egg spherical, thick-shelled,

Pyriform apparatus cither conical or terminat>

ing in two horns, numerous teflexed filaments

attached to apex of pyrifarm apparatus.

Sperm first appears in external and internal

seminal vesicles in ¢.105th proglottis; seminal

receplacle fills will sperm tn c.1 10th proglot-

tis, after male system commences to function,

Vagina does not atrophy following insemina-

tion. Ovary fully developed from ¢.140th to

150th proglottis, involutes over 2-3 proglot-

tides, Uterus begins to fill with eggs im-

mediately after involution of ovary (¢.1 50th),

Discussion: Progamotaenia diephana was te

described very briefly by Beveridge (1976)

based on a single specimen assumed to be type

Material aod a small number of fragmented

specimens from a captive wombat. Although

the latter collectian suggested that Laxiorhinuy

Jatifrens ovight be the usual host of FP. alu.

phana, no material had been seen from free-

living hosts, and the very closely related ces-

tode, FP. festive, had been collected from the

bile ducts of free-living Vombatus ursinus

(Beveridge 1976), Subsequently, collections of

cestodes fram LL. latifrons in South Australia

were tentatively identified ag P, festiva (Rudel-

phi 1819) as they did not conform exactly to

the description of PF. diaphana, and doubt was

thrown on the status of P. dfuplana itself

(Presidenic & Beveridge 1978). Abundant col-

lections now do hand inilieate thar P, afop hana

is a distinctive form, probably warranting

specific status, and that doubt as tr the identity

of Presidente & Heveridge’s maternal was doc

to a lack of apprectation of the extent of Varia-

bility in the species.

The present redescription differs from that

of Beveridge (1976) in a number of potnts.

A prominent external seminal vesicle was pre

sent in the new nvaterial, but was stated as

being absent in the earlier description, The

number of testes per group was previatisly re

ported as 17-21, but in the new material &

18-33 per group or 39-53 per proglottis. Pan

of this variability is due simply to vanahion

between individupl cestudes, In two srebilwe

examined, the range aml mean number of

testes per proglottis based on examination of

LO proglottides in each strobiln was 32-463

(56) anc 39-53 (46), Number of testes per

Proglottis in the related P. frstiva is FU-140,

so that in spe of the vartubiliny, testis. wuo-

ber is still a uselul uethod of distiuguistung the

species,

In the type specimen redescribed by Bever-

idge (1976) early tasemination of proglottidce

was followed by vaginal atroghy. This pheno-

menin wis not recorded in the orginal des

éription (Zschokke 1907) and was not present

in the ofher material described hy Beveridge

Figs 24-29, Progamotacnia diaphana (Zschokke). 24. transverse histalogical section uf Larcral region of

proclottis. showing cirrus sac, uterus and muscilawire; 25. mature proghottiss 26. mature pravhsides

showing vuriation in proglottis shape and testis distribution; 27, gravid proglottiss 2h, scelux; 29,

mature proglottis showing variation in testis distribution. Scale lines 0.1 mm,

78 I, BEVERIDGE

(1976), In the new material, insemination in

variably occurs after the male reproductive

system of a particular proglottis has stunted to

function and vaginal atrophy sever occurs

following insemination, The distal vagina js

frequently difficult to see in moulited spect-

mens, so fragments of the type material were

serially sectioned, showing thal the vagina re-

mitines? intact in past mature proglottides and

suggesting that Beveridge’s interpretation based

on the single whole mount preparation was in-

correct. BeVeridge’s (1976) suggestion that

vaginal atrophy could vary within a species

should therefore be ignored, The sugrestion

has alsa proven incorrect in the case of P,

laygorchestis and P. tylogaie (Heveridge &

Thompson 1979); species which were initially

confused linder the one name.

Two diagrams of the egg of P. diaphana

were given by Beveridge (1976), one showing

the pyriforin apparatus ending in two horns

and the other showing an undivided pyrilonm

apparatus, Both forms ure present im the sew

material but, being unmounted, it is possible

to rail the eggs under a coverslip and show that

there are indeed two different types and that

they are Wot the same form viewed from dif-

ferent aspects (Beveridge 1976). The undi-

vided form ts identical with that found in P,

festive and the divided form may merely be a

developmental stage (Beveridge 1976), since

it occurs in much lower numbers, This form

of pyriform apparatus was illustrated by Bohm

& Supperer (1958).

The presence of dark pigment in the scolex

of P, diaphana was first reported by Béhm &

Supperer (1953), and ts present in the single

scolex antony the type material as well as in

all lots of new material. The pigment, how-

ever, is not invariably present and cannot

therefore be used as a distinguishing character.

Beveridge (1976) Hsted a number of fea-

tures which distinguished P, diapkana from

the related FL festive, Of these, the presence uf

proterdgvny ad vaginal atrophy should be dis-

carded, while the shape of the uterus requires

a subjective assessment and is therefore of

doubtful value, ‘The two species differ in the

frequent presence of dark pigment jn the sca-

lex of F. diaphane and differences in the num-

her of festes per penglottis, allowing for the

considerable variation which occurs in’ hoth

species. Ly view of the present redescription,

P. digphane probably warrants continued

specific rank, and the specimens described tn-

der the nanic P, festive from L, latifrons by

Presidente & Beveridge (1978) should be re-

named FP. dlaphana. However, Beveridge

(1976) has pointed to the exlensive Variation

in specimens of P. feytiva from various host

species, and it is cyident that a reassessment

of this taxon and P. diaphana will be necessary

when life histories are known and cross infec-

tion experiments can be undertaken.

The data presented above establish 1, lati-

Jrons as the usual host for P. diaphana. Rohm

& Supperer (1958) reported P. didphana from

a captive Vombatus ursinus in Europe, but

subsequent correspondence by a colleague with

Supperer established that this animal was in

fact LL. latifrons (Presidente & Beveridge

1978), and had earlier been misidentified. In

his original description, Zschokke (1907) gave

no details as to how he obtained his speci-

mens, and gave the bost name as Phascolomys

wombet, a name which is now placed as a

synonym of V. ursinas, but which could have

becn applied to any of the species of wombats.

If, as indicated by data associated with the

material considered now to be type material,

the species was initially collected by E. Angas

Johnston, then ZL, Jatifrons may be the type

host. Angas Johnston was a doctor afd ama-

teur naturalist who lived in Adelaide.

lrogamotacnia zschokkei (Janicki, 1909)

Material examined; From Onychogalea frae-

nata: 1 specimen, Dingo, Qld, 12.vit.1975,

J. E. Nelson; 5 specimens, captive atimals

originate from Dingo, Qld, March 1978,

19.i,-1979, T, Beveridge: 8 specimens, same

data, 26.yii,|979, R, Speare. From Onveho-

gelee wnguifera: 4 specimens, “Kimberley

Ranges", WA. 3Lviill976, 6.xi1.1976, L,

Keller; 2 specimens, Chadshunt Stn, Qld,

6 ili 1879, R, Speare and P. M. Johnson.

From Lagorchestes conspicillatus: 5 speci-

mens, Inkerman St, Qld, 7.i%.1979, 141.1979,

P.M. Johnson; 3 specimens. Mingela, Qld,

10.v.1979, | Beveridge. From Thylogale stie-

inaneat 10 specimens, El Arish, Qld, 30, vii.

1978, |. Beveridge, From Petrogale penictllata:

3 specimens. Hervey’s Range, Townsville,

Old, d.iv.1979, 1. Beveridge. From Macropus

agilis: 5 specimens, Marrakai Plains, N.T,

29,jx.1973, L, Corner; |3 specimens, Towns-

Ville. Old, T5.vi,1978, 1, Beveridge,

Discussions Onvehagalea fraenata, O. ungui-

Jera and Meecropus aeiliy are new hosts for

Progamoteenia zchokkei, Part of the material

listed above from M. agilis was identified

erroneously as P. Jagorchestis by Beveridge

SPECIES OF PROGAMOTAENIA (CESTODA: ANOPLOCEPHALIDAE) 7

(1976). M. agilis is not a host of P. lagorches-

tis or of P. thylogale, a species which was con-

fused under the former name by Beveridge

(1976), Further specimens of P. zschokkei

from Thylogale stigmatica and Petrogale peni-

cillata confirm earlier reports from these hosts

based on rather poorly preserved material

(Beveridge 1976).

There was considerable size variation in the

specimens of P. zschokkei examined. Those

from OQ. Jraenata measured 95-120 x 11-12

mm; specimens from Q. unguifera were latger,

measuring 380-460 x 8-12 mm. Specimens

from L, conspicillatus were 160-170 mm long

and varied from 8-13 mm in width, Cestodes

from M, agiliy were long (130-185 mm) but

only 4-6 mm wide while specimens from P,

penicillata and T. stigmatica were the smallest,

measuring 58-61 x 2-3 mm and 50-90 x 2-3

mm respectively. In spite of the great differ-.

ence in size, there were no significant differ-

ences in internal morphology. The size differ-

ence may be due to the influence of the host,

but experimental infections will be needed to

demonstrate whether this is the cause of the

observed differences, or whether a species com-

plex exists. Similar size variation has been

noted in P. festiva and P. macropodis (Beyer-

idge 1976),

Acknowledgments

Thanks are due to M. Gaughwin, R. Speare

and P, M. Johnson for collecting specimens,

or for supplying wallabies for dissection,

References

Baer, J. G. (1927) Monographie des cestodes de

la famille des Anoplocephalidac, Bull. bial. Fr.

Belg. Suppl. 10,

Beveriwor, T, (1976) A taxonomic revision of the

Anoplocephalidae (Cestoda: Cyclophyllidea) of

Australian Marsupials, Aust. J, Zool. Suppl.

(44), pp. 110.

—— (1978) Progamotaenia tuficola sp, nov.

(Cestoda; Anoplocephalidae) from the red kan-

garoo, Macropus rufus (Marsupialia). J. Para-

sitol. 64, 273-276,

& Thompson, R.C. A. (1979) The anoplo-

cephalid cestode parasites of the spectacled hare

wallaby, Lagorchestes conspicillatus Gould,

1842 (Marsupialia: Macropodidae), J. Helmin-

thal, 53, 153-160,

Roum, L. K. & Suppercr, R. (1958) Beitriige zur

kenntnis tierischer Parasiten (1, Zentralbl, Bak-

terlal, Abt, 1, Orig, 172, 298-309,

Jonnston, T, H, (1912) Notes on some entozoa.

Proce. R. Soe. Qld, 24,, 63-91,

Lewis, R. C. (1914) On two new species of tape-

worms from the stomach and small intestine of

a wallaby, Lagarchestes conspicillams, from

Hermite Island, Monte Bello Islands, Proc, zool,

Soc, Lond., 419-433,

Nyse, O, (1917) Australische Cestoden. Re-

sults of Dr E. Mjéberg’s Swedish Scientific Ex-

peditions to Australia, 1910-1913, Kungl.

Svensk. VWetenskapsakad. Hand], 52, 1-48.

Presiente, P, J, A, & Bavertmce, J. (1978)

Cholangitis associated with species of Proga-

molaenia (Cestoda; Anoplocephalidae) in the

bile ducts of marsupials. J. Wildl, Dis. 14, 371-

377.

Rauscn, R. L. (1976) The genera Paranoploce-

phala Lithe, 1910 and Anoplocephaloides Baer,

1923. Ann. parasit, hum. comp, 51, 513-562.

Sanpars, D. F. (1957) Redescription of some ces-

todes from marsupials. IT. Davaineidae, Hy-

menolepididac and Anoplocephalidac, Arn,

Trop, Med, Parasitol, 51, 330-339.

ZSCHOKKE, F, (1907) Moniezia diaphana n. sp.

ein weiterer Beitrag zur Kenntnis der Cestoden

aplacentaler Saugetiere. Zentralbl. Bakteriol,

Parasitenkd, 44, 261-264,

BEVERIDGEA NEW GENUS (NEMATODA: STRONGYLIDA) FROM THE

AGILE WALLABY FROM NORTHERN AUSTRALIA

BY PATRICIA M. MAWSON

Summary

Beveridgea n.g., type species B. corneri, n.sp., is close to Cloacina, differing chiefly in the much

longer buccal capsule, and in the shape of the bursa, which is not joined ventrally. B. corneri has

been taken from Macropus agilus, only on Cape York Peninsula, Queensland.

BEVERIDGEA NEW GENUS

(NEMATODA; STRONGYLIDA)

FROM THE AGILE WALLABY FROM NORTHERN AUSTRALIA

by ParriciA M. MAwson*

Summary

Mawson, P. M. (1980) Beverideea new genus (Nematoda: Strongylida) from the Agile

Wallaby from northern Australia, Trans. R, See, S, Aust. 10404), 61-82, 30 May, 1980,

Beveriigea wg.. type species BL corneri, msp, is close to Cloacina, differing chiefly in

ihe much longer buceal capsule, and m the shape of the bursa, which is not jammed ventrally.

B. corner? bas been taken from Macrapus agilis, only on Cape York Peninsula, Queensland,

Bevyeridgea fg.

Cloacininac: cephalic roll well developed;

submedian cephalic papillae elongate, bi-

seymented, buccal capsule cylindrical, longer

than its diameter, votehed along anterior

border; leaf crown of eight elements arising

near anterior end of buccal capsule; cervical

papillae thread-like; dorsal oesophageal gland

opens into base of buccal caviry-

Male; spicules elongate, alate, bursa not deeply

lobed, ventral lobes almost separate; ventral

rays together, ventro-lateral ray separate from

other faterals, externo-dorsal ray arises

separately, dorsal ray divides twice, Guberna-

eulum present

Female: tail short, conical; vulva near anus,

junction of ovejectors parallel with long axis

of body,

Parasites of stomach of macropodid marsu-

pials.

Type species: B. corneri n. sp.

Beveridgea has been referred to the Cloaci-

ninae sensu Lichtenfels (1980) because of the

type of Jeaf crown and cephalic papillae, and

the fact that the dorsal ocsophageal gland opens

directly into the base of the buccal cavity.

Tt is distinguished from Cloacina Linstow,

1898. mainly by characters of the buccal cap-

sule, which is longer, and of the leaf crawn,

the elements of which arise from the anterior

end of the capsule wally moreover, in Clawelna

the ventral lobes of the bursa are joined.

Beveridgea cormeri o.sp.

FIGS 1-7

Host and loealitiess Macropes agilis Gould, From

Elizabeth Downs Station (1ype locality) and

from Stones Crossing, Wenlock R., Qld. Holo-

type male and allotope female deposited in

South Australian Museum (V19I0),

* Department of Zoology, University of Adelaide,

Box 498, G,P.O., Adelaide, S. Aust. 5001.

This species was taken from at least three

host animals, but very few were present in

each; all are young worms, the females with-

out eggs in the uteri, The species hus not been

found among stomach worms from M, agilis

from more southerly parts of Queenslabd or

from the Kimberley District of W.A.

Length of males 4.7-5.7 mm, females

4.9-5.3 mm. Labial collar well developed,

slightly Jobed anteriorly. Cephalic papillae of

two segments, distal distinctly shorter than

proximal, Buceal capsule 40-50 ym long, its

anterior border notched, its posterior border

lobed, following contour of anterior end of

oesophagus. Fight elements of leaf crown

anise from antetior 1,, of wall of buccal cap-

sule, and end in points around mouth. In

posterior ), of buccal capsule small jeregularly

pluced denticles project into buceal cavity.

Oesophagus 480-520 ym long in male, 440-

$50 pm in female, cylindrical in anterior half,

then slight swelling preecdes position of nerve

rig, and posterior portion widens towards

base, In median swelling small tooth projects

into Jumen. Dorsal oesophageal gland distinct,

openiig on a prominence at anterior end of

dorsal section of oesophagus.

Nerve ring lies just posterior to median

swelling of oesophagus; exeretory pore near

base of oesophagus: thread-like cervical

papiliaeg 125-130 (4) and 120-140 (2) froro

anterior end,

Male: bursa with characters of genus. Dorsal

ray divides just hefore midlength, and final

branches very short. Genital cone short,

flanked by two lateral “balloons” of apparently

inflated cuticle. From base of dorsal ray single

digitiform ‘papilla’ projects into cavity of

bursa (Fig. 6).

Female: tail 150-200 pm long, vulva 220+

310 pm from posterior end, Eggs absent.

82 PATRICIA M, MAWSON

100 jim

Figs 1-7, Beveridgea corneri n.sp. 1 head, lateral view; 2. anterior end, dorsal view; 3. oesophageal

region; 4, 5 and 6, bursa in dorsal, ventral, and lateral views respectively; 7. posterior end of

female. (Figs 4-6 to same scale).

Acknowledgments Dept of Tropical Veterninary Science, James

The material for this study was kindly Cook University of North Queensland). It was

given to me by Dr I. Beveridge (then of the collected by him and by L. Corner.

References

LICHTENFELS, J. R. (1980) Keys to genera in the Linstow, O. von (1898) Nemathelminthen gesam-

superfamily Strongyloidea. CIH Keys to the melt von Prof. Dr F. Dahl in Bismarck Archi-

nematode parasites of vertebrates, No. 7. pel. Arch. f. Naturg. 1, 281-291.

Commw. Agric. Bur., Farnham Royal.

NON-MARINE MOLLUSCS FROM DOLOMITIC LIMESTONES IN THE

NORTH OF SOUTH AUSTRALIA

BY N. H. LUDBROOK

Summary

Non-marine molluscs, from the type section of the Etadunna Formation at Lake Palankarinna

(KOPPERAMANNA 1:250 000 map sheet), and from dolomitic limestones on the BILLA

KALINA and TARCOOLA 1:250 000 map sheets are described and correlated with those occurring

in northern Australia. Etadunna Formation molluscs from Lake Palankarinna are land snails —

Bothriembryon praecursor and Meracomelon lloydi — while those from near “Billa Kalina” and

“Malbooma” and also from Lake Woorong on the COOBER PEDY 1:250 000 map sheet are

freshwater species of Syrioplanorbis, Physastra and Rivisessor. The dolomitic limestones are

considered to be of Miocene age.

NON-MARINE MOLLUSCS FROM DOLOMITIC LIMESTONES IN

THE NORTH OF SOUTH AUSTRALIA

by N. H, Lupprook®

Summary

Luperook, N, H, (1980) Non-marine molluscs from Miocene dolomitic limestones in the

north of South Australia. Trans, R. Soc, S. Aast. L04(4), 83-92, 30 May, 1980.

Non-muriine molluscs, from the type section of the Etadunna Formation at Lake Palan-

karlnna (KOPPERAMANNA 1:250-000 map sheet), and from dolomitic limestones on the

BILLA KALINA and TARCOOLA 1:250000 map sheets are described and correlated with

those occurring in northern Australia. Etadunna Formation mollitscs from Lake Palankarinina

are land snails — Berliriembryon praccursor and Meracomelon lloydi — while those from neat

“Billa Kalina” and “Mualbooma" and also from Lake Woorong on the COOBER PEDY

1.250000 map sheet are freshwater specics of Syrioplanarbis, Physasrra and Rivisesser,

The dolomitic limestones are considered to be of Miocene age

Introduction

In describing fossil pon-marine molluscs

from northern Australia, McMichael (1968)

cited sone of the species as occurring also in

the “Etadunna Formation, Billa Kalina Station,

South Australia.” ‘Tabulating the localiues.

lithology and faunas of samples examined by

MeMichael, Lloyd (1968) similarly attributed

to the Etadunna Formation, Tirari Desert,

three species, two of which came from Lake

Palankarinna and one from Billa Kalina, The

present paper seeks to correct the unfortunate

confusion of two widely separate localities,

sbown on Figure 1, and to distinguish between

those molluses which occur in the type section

of the Etadunna Formation at Lake Palan-

karinna and those in the dolomitic limestones

cropping out north of “Billa Kalina” Home-

stead. The fossil content of dolomitic lime-

stones from near “Malbooma 0.5.” is also

placed on record,

All the material studied is in the Palaeonto-

logical Collection of the Geological Survey of

South Australia, All may references are to the

Geological Atlas Series,

Specimens from both Lake Pulankarinna

and north of “Billa Kalina” were sent to

MeMichael at the Australian Museum in 1963

with references to published data on the Eta-

dunna Formation and a note to the effect that

"the dolomite containing Planerbiy from Billa

Kalina is not necessarily to be correlated with

the Etadunna,” In official correspondence,

McMichael tentatively identified the Etadunna

gastropods respectively us belonging to the

genus Bothriembryen anid similar to Jand

*e/e Deparrment of Mines & Energy, P.O, Box

151, Eastwood, 8S. Aust. 5063.

snails of the genera Meracomelan and Sinn

melon, probably the former, ynd Lhe material

from Rilla Kalina as a large Planorbis-like

shell,

In 1965, Etadynna specimens were again

sent to McMichael to supplement his studies

of the northern Australian fauia, No material

from Billa Kalina was included, McMichael’s

(1968) reference to the occurrence of certain

species in the “Eladunna Formation, Billa

Kalina Station" seems to originate in noles he

made m 1963 when he had specimens from

both localities.

One of the Unfortunate cousequences of the

error is (hat the gastropods of the type seetion

of the Etadunna Formation at Lake Palan-

karinna have been only obscurely recorded,

Moreover, the molluscs from the Etadutna

Formation are land snails, while those from

Billa Kalina are freshwater. The only Iime-

stones containing both land and freshwater

moltluses (tabulated by Lloyd 1968) appear to

be in the Deep Well area of Central Australia

and the Carl Creek Limestone of the Rivers-

leigh area, Queensland

Motluses from the Etadanna Formation

The molluscs from Lake Palankarinna, south

of Cooper Creck, 23 km SW of “Etadunna™

(lut, 28'48'S, long. 138°25°E_ locality sample

number 6540 RS 39, KOPPERAMANNA

1:250 000 map sheet) were collected by R. H.

Tedlord from nodular dolomilic limestone at

the base of member 2e, Etaduijna Formation

(Stirian er al 1961). Additiumal specimens

were collected by 1. M. Lindsay in 1970. They

therefore come rom tow in the formation,

some 5 mi above the base, although gastropods

have been recorded by Stirton and his col-

VERTICAL SCALE SECTION AT

("METRES LAKE PALANKARINNA

50-0

WINDRIFT

DUNES

KATIPIRI SANDS

Cross—bedded sands

Gypsum

TIRAR|

FORMATION

TYPE LOCALITY

Red argillaceous

sandstone

PLEISTOCENE

MAMPUWORDU

SANDS

TYPE LOCALITY

Channel sands

ETADUNNA

FORMATION

TYPE LOCALITY

Green arenaceous

® claystone

By Calcareous mudstone

6 Green argillaceous

sandstone

Green arenaceous

claystone

4 Green sandstone

ee)

Grewn claystone

Gastropods

Calcsreous mudstone

and dolomitic limestone

Gastropods

Green sraillaceoua

sandstone

WINTON

FORMATION

Grey argillaceous

sandstone

Adapted from Stirten.

Tedlord and Miller, |?é!

Bin JPY

—

FIGURE 2

N, H. LUDBROOK

1797 13)"

133" NT

BILLA KALINA

'Malboora 0,

KILOMETRES

LOCALITY MAP

FIGURE 1

139° Ou

——_!

Pe 2a |

KOPPERAMANNA

Lake Patankarinna

SECTION AT

“BILLA KALINA"

Ambrose and Flin, 197)

Dolomite limestones

with dolomite

intraclasts

Clays and shales

Sand lunses with

quartzite cobbles

and boulders

Discenformity

BULLDOG

SHALE

Clays and shale with

sand lenses and

qQuartzle cobbles and

boulders

SJ. Doly, 1979

BO-A4 S.A

SECTION AT

"“MALBOOMA"

Dolomitic Jimestunas

with dolomite

intractasts

Clays and shales

PIDINGA

FORMATION

Garbonaceous

sandy clays

Deportment ol Mines ond Ener

MIOCENE NON-MARINE MOLLUSCS 85

leagues fram calcareous mudstones at both the

basy and top. The measured stratigraphic type

stetion at Lake Palankarinna, redfawn after

Stitton ef al. is shown in Figure 2.

In the opinion of Stirton et a/, (1961), the

sequence of dolomitic limestones, calcareous

mudstones and claystones with intraforimea-

tional breccias represents deposition in a shal-

low-water lygoon with repeated exposure and

drying. The green claystones and argillaceous

sandstones have yielded the important Ngapa-

kaldi vertebrate fauna which contains lungfish

and Water birds. [ft includes also diprotodonts

and macropodids which appear to have heen

entrapped in hoggy clay. Gastropods in the

dolamitic Iimestones are in the form of moulds

and casis, many of which are freed from the

mateix, They seem to be locally common and

arcearious, but belong to only two species,

Bothriembryon praecursay MeMichael 2nd

Meracomelan lloydi McMichael. Both species

are related to land snails typically inhabiting

and parts of the State — Sothrieimbryen bar-

rei ihe Nullarbor Plains and Mferdeornelon

spp, the Northern Flinders Ranges. As no

freshwater shells have so far been found with

them, they are presumed to represent the

drying-out periods of deposition of the Bta-

dunna Formation postulated by Stirton and his

colleagues,

The possible relationships between land

snails from non-marine deposits in and near

Hobart and species of Bathriembryen und

Meracomelon. occurring in the Etadunna For-

mation were considered by McMichael.

Examination of the Jimited amount of

material now available from Hobart, discussed

in the systematic section, has failed to estab-

lish similarity between the Tasmanian species

in the Geilston Travertine and those fron the

Etadunna Formation,

Mollises from the Billa Kalina area

The following deseriplion of the planorbid-

bearing limestoues from worth of “Brile

Kalina” Homestead (locality ind simple num-

hers 6148 RS 62-73, 87, BILLA KALINA

1;250000 map sheet, tat, 29°53'S, long,

136° 11'E) is modified from Ambrose & Flint

(1979)1,

t Ambrose, G. J. & Flint, R. B. (1979), A regres-

sive Tertiary Tyke system and silicitiod strand

lines, Hilla Kalina area, South Australia S.A.

Dept. Mines & Energy Rept 79/104 (Cunjub-

lished).

Tertiary sediments neat “Billa Kalina” form

a thin capping, maximum thickness 13 m, on

shales and conglomeratic sands of Early Cre-

raceous Bulldog Shale. A fesistan! dolomitic

limestone within the Tertiary sequence over-

lying the more-casily eroded shales results in

flat-topped plateaux and mesas.

An idealised sequence (Fig, 2) comprises a

very thin basal sand horizon containing quart-

zite clasts derived from erosion of the Creta-

ceous sediments, This is overisin hy approxi-

mately 5 m of green dolomitic and oceasion-

ally palyporskite-bearing ¢lays, which are in

turf overlain by 1.5 nt of white fossilifeeous

limestones and dolomitic limestones.

Samples with planorbids, ta which the num-

ber 6138 RS 87 has heen assigned, were first

bollected from these limestones in 1958 by

H. G. Roberts during reconnaissance mapping

tor Clarence River Oil Syndicate. Subsequent

collections (6138 RS 62-73, containing hydro-

bids) were made in 1974 by G. J, Ambrose

and R, B. Flint during mapping of the BILLA

KALINA 1;250000 mup sheet from three

localities within 4 distance of 1.5 km from 3,5-

40 km NNW to N of “Billa Kalina”, The total

amount of material is not large, snd the known

Fauna is limited to four species—an undescribed

species of Roivessor occurring in samples 6138

RS 62-73. Syeioplaterbiy heardmani, Syrio-

plunorhis sp., and Physastra padlagee, eithee in

crowded masseg or scattered throughout the

matrix, These were freshwater inhahitunts of

or were washed into the Tertiary lake postu-

lated by Ambrose and Flint,

The Tertiary sediments on Billa Kalina and

Millers Creek Stations have: been correlated,

on a lithological basis, with the Etadiinna For-

mation of the Lake Eyre Basin and the Namba

Purmanon of the Tarkarooleo Basin (Jessup &

Norris 1971; Ambrase & Flint 1979*)_ Jessup

& Norris divided what they considered to be

the Etadunna Formation in the Billa Kalina-

Millers Creek area into two members — a

jower Bula Kalina Clay Member.and an upper

Millers Creek Dolomite Member, A revision

of this nomenclature is presently being pre-

pared by Ambrose and Flint, and, pending its

publication, the Billa Kalina Clay Member and

the Millers Creek Dolomite Member are here

regarded as units of an unnamed formation.

The molluscs in the dolomites provide the only

direct evidence so far obtained for correlating

them with other formations of known Tertiary

age,

8h N. H, LUDBROOK

Material from “Malbouma Outstation" arca

Tertiary fossils were first collected in [his

area in 1979 by R. B. Flint, S.J. Daly and

A, FB. Crooks (locality and sample nunbers

5736 RS 47-52 TARCOOLA 1:250000 mip

sheet. Jat, 30°39'S, long, 134°05°E) A bret

veological description is provided by S. J, Daly:

‘Possible Jute Teniary sediments west ol

*Malbooma O.S." crap out poorly, and fore

low cises which are veneered by calerete. The

best exposures are in radiway cullings on the

Trans Australia Railway Line. The sequenes,

thought to he approximately 6 4 thick, overs

lies carbonaceous sandy clays and sands of the

Middle Eocene Pidinga Formation” (Fig. 2).

In a railway cutting 15.5 km west of “Mal

booma 0,8." dark olive-green clays with red

and yellow mottling 4re overlain by white-

yellow fossilileraus dolomitic Jimestones which

are fragmenta! at the top. The base of the se

quence is not exposed, No fossils were pre-

viously known an the sequence”.

The limestunes are sparsely fossiliferous with

scatiered impressions, fragments and casts of

Rivisessor sp. in a pelletal matvix, Oceasional

oogonia of a charophyte are also present, The

enviloament was lacusirine, probably similar

to and contemporaneous with that at “Billa

Kalina”

Delomitic limestone from Lake Woorang

ln March 1980. fossiliferous dolomitic

limestone (sumple 5739 RS 23) was collected

by M. C, Benbow, G, W, Kricg and P. A,

Rogers from the southern lake of Lake Woo

rong, 32 km west of Lake Phillipson (lat.

29°36 06"S, long. 134°07'54"E, COORBER

PEDY 12250000 geological map sheet), The

hard dolomitic limestone, with dolomite clasts

find occasional scattered casts and moulds of

small gastropods, is similar ta material val-

lected from near ‘Billa Kalina”, Although pre-

servation is very poor, by analogy with the

Billa Kalina and Malbooma material, the easts

and moulds cam be identified as the freshwater

gastkopodsy Rivisessor sp. and Plrysastrey redin-

eae. The material was collected too recently

for the Jweality to be included uw cither Figure

1 or Figure 2, COOBER PEDY sdjuins TAR-

COOLA on the suwth and BILLA KALINA

on the east.

Age aud correlation of the dolomitic

limestones

The age of the Btadunta Formation has

been determined by W. K, Harris on unpub-

lished palynolagieal data as Middle Miocene

(Callen & Tedford 1974, Callen 1977). ‘The

Etadunta land matluses Bariwiembrven prae-

cursor und Merecemelon llevdi occur, either

separately ar together, in unnamed Tertiary

limestones near “Deep Well” SSE of Alice

Springs and in the Carl Creek Limestone N

and SE of “Riversieigh,” Queensland.

The molluscs in the limestones in the Billa

Kalina, Malhooma and Lake Wooronu areas

ate from a freshwatec environment and do tot

provide direct correlation with the Etudonna

Formation. They are felated to one another

by the presence of Rivivessor sp. The sniall as-

semblage of Syrioplanorhis hardmani and Phy-

saxira redingae permits correlation of the dolo-

nites near “Billa Kalina” with the White Moun-

tain Formation of the Ord Basin in north-

western Australia, the Arltunga Beds, un-

named limestones of Ihe "Deep Well” area, in

the Alice Springs area, ynd the Carl Creck

Limestone, Horse Creek Formation and Brun-

ette Limestone in Queensland, All of these have

been regarded by Lloyd (1968) us of Miocene

age but nol necessarily correlates. ‘The lime:

stones at Billa Kalina and Malbnoma afte there-

fore vonsidered to be also of Miocene age. bul

not hecessarily exact correlates of the lower

part of the Btadunna Formation.

Systematic descriptions

Class GASTROPODA

Subclass PROSOBRANCTUA

Order MONOTOCARDIA

Fig. 3 (a-e) Bothrieubryon proceursur, Btadunna Vormation, Lake Palankiwrinm, (2) M273811) x 1,2,

large specimen, (b, cy M273803), showing fut intergal spiral ribbing. fd, e) Mt74403), murray

specimen with axial ribs, w x 12. (f1) Meracomelon loydi, Fladunna Formation, Lake Palankarinns

(f) M2740. apertural view. (2) M2740), umbiltest view, (h) M27410 11. apical view. (1) M2741(1),

umbilical view. (j) M2743, aperturul view. (ky M2743, apertural view (1) M2743, 1mbilical view,

(m-u) Syrieplanarbis hardinant, Billa Kaling Oreo) M2746(1), broken specimen giving natutal sec-

tion showing usymmetrical Bperlure (p, a) M2402) lawer and upper sides, fr, 4) M2746(3}

lower and upper sides, (6) 4357901), (1) M3S79(3) moulds and casty in limestone, (yw) Syrlas

planorbiy sp.. Billa Kajima tv} M3580(1), showing spiral ribbing. (w) M3SR0(2), shawing syin-

metrical aperture. (x) Plivsestra rodinvac, Billa Kalina, M358107), (¥, 2, ga) RiiLeessar specimens

an Beste (v) 6138 RS 70, Billn Kalina, Ge) 6138 RS 7), Billy Kalina. (4a) 9736 RS 48, Mal.

OMA,

MIOCENE NON-MARINE MOLLUSCS

88 N. H. LUDBROOK

Suborder TAENIOGLOSSA =

TROPODA

Superfamily RISSOACEA

Family HYDROBIIDAE

Genus RIVISESSOR Iredale, 1943

MESOGAS-

Rivisessor sp.

FIGS 3y, z, aa

Material: Numerous specimens scattered through-

out the matrix of samples 6138 RS 62-67 from 4

km NNW of “Billa Kalina”, 6138 RS 68-70 from

3.5 km N of “Billa Kalina” and 6138 RS 71-73

from 4 km N of “Billa Kalina”, casts and moulds

in matrix of samples 5736 RS 47-51 15.5 km W

of “Malbooma O.S.” and 5736 RS 52 9 km W of

“Malbooma O.S.”

Description: Shell small, smooth, thick, solid,

whorls 4 to 5, moderately tumid, suture im-

pressed. Aperture oval, entire, oblique; last

whorl 3/5 height of shell, Height 5, diameter

2.5, height of last whorl 3, height of aperture

1.5 mm. Maximum height estimated from an

imperfect natural section 7, diameter 3 mm.

Distribution: Limestone cappings at Billa

Kalina, localities 6138 RS 62-73 (BILLA

KALINA 1:250000 map sheet) and Mal-

booma, localities 5736 RS 47-52 (TAR-

COOLA 1:250 000 map sheet).

Habitat: Living species of Rivisessor com-

monly inhabit streams, lagoons and ponds.

Order BASOMMATOPHORA

Superfamily LYMNAEACEA

Family PLANORBIDAE

Genus SYRIOPLANORBIS Baker, 1945

Syrioplanorbis hardmani (Wade)

FIG 3 m-u

Planorbis hardmani McCoy. Hardman 1885: 7, 15

(nom. nud.)

Planorbis hardmani (Foord) (sic) Wade, 1924:

29, pl. 1

Planorbis hardmani Wade. Chapman 1937: 61, pl.

6, figs 1, 2

Syrioplanorbis hardmani (Wade).

1968: 141, pl. 10, figs 6-8

Material: 15 internal casts GSSA M2746; numer-

ous internal casts and moulds in matrix, M3579

(locality 6138 RS 87, 4 km N of “Billa Kalina”).

The species was described adequately by

McMichael. All specimens show the slight

asymmetry with a deeply concave upper sur-

face and shallowly concave lower surface typi-

cal of the species, Dimensions of the ten mea-

surable specimens are consistent with those of

the types from White Mountain Hills, Western

Australia and specimens from south of Herr-

mansburg in Central Australia:

McMichael

GSSA Reg. Diam. Height Diam./Height

No. (mm) (mm) ratio

M2746(1) 20.0 7.4 2.70:1

M2746(2) 18.0 7.0 2.57:1

M2746(3) 16.4 5.4 3.04:1

M2746(4) 11.4 5.0 2.28:1

M2746(5) 13.7 6.0 2.28:1

M2746(6) 12.0 5.5 2.18:1

M2746(7) 12.4 5.4 2.30:1

M2746(8) 11.9 6.0 1.98:1

M2746(9) 11.4 5.5 2.07:1

M2746(10) 9.6 4S 2.13:1

Average 13.68 5.77 2.37:1

Type locality: Trig J40, 15 km E of N of “New

Ord River’, White Mountain Hills, lat.

17°15'37"S, long. 128°57'57"E, LISSADELL

1:250 000 map sheet, Kimberley District, W.A.

White Mountain Formation, ?Miocene.

Distribution: The localities cited by McMichael

are here reinterpreted from Lloyd (1968),

Wells et al. (1970) and Playford et al. (1975):

Western Australia-White Mountain Forma-

tion, White Mountain Hills 15 km E of N of

“New Ord River’, LISSADELL 1:250 000

map sheet; Northern Territory—NT 406, un-

named formation, 6 km W of Running Waters,

42 km S of MHerrmansburg, HENBURY

1:250 000 map sheet; NT 409, unnamed for-

mation, 16 km NNE of ‘Deep Well”, 61 km

SSE of Alice Springs, RODINGA 1:250 000

map sheet; NT 417, unnamed formation, 16

km NE of Undoolya Gap, 45 km E of Alice

Springs, ALICE SPRINGS 1:250000 map

sheet; NT 422, Arltunga Beds, 3.2 km SW

of Arltunga airstrip, ALICE SPRINGS

1:250 000 map sheet; NT 423, Arltunga Beds,

Arltunga airstrip, ALICE SPRINGS 1:250 000

map sheet; AS 234, unnamed formation, 24

km SE of “Todd River” H.S., ALICE

SPRINGS 1:250000 map sheet; AS 235,

unnamed formation, 21 km ESE of

“Todd River” H.S., ALICE SPRINGS

1:250000 map sheet; Queensland — Q9,

Horse Creek Formation, 25.6 km SE of

“Springvale” H.S., SPRINGVALE 1:250 000

map sheet; BT 169, Brunette Limestone, 45.6

km N_ of “Rockhampton Downs” H.S.,

ROBINSON RIVER 1:250000 map sheet;

South Australia — 6138 RS 87, unnamed for-

mation, 4 km N of “Billa Kalina”, BILLA

KALINA 1:250000 map sheet.

The genus is recorded from the Late Oligo-

cene of Europe and the Far East, but as liv-

ing only in Lebanon and Syria. No living re-

presentatives are known from Australia.

Habitat: Freshwater.

MIOCENE NON-MARINE MOLLUSCS 89

Syrioplanorbis sp,

FIGS 3y, w

Material; Two internal casts GSSA M3580(1-2),

locality 6138 RS 87, 4 km N of “Billa Kalina’

HS.

Deseviption: Sinistral, discoidal, both upper

and lower surfaces deeply and fairly broadly

umbilicate, Whorls 44, regularly increasing,

laterally somewhat compressed and inclined to

be angulate af upper and tower curvature.

Sutures deeply impressed. Shell unknown, Sut

cast showing three conspicuous spiral ribs on

lateral surface, Aperture more or less sym-

metrical, moderately arched,

GSSA Reg. Diam, Height Diam./Height

Na. (mm) (mm) ratlea

M3580 1) 12.2 63 1.94:1

M3580(2) 10,2 5.0 2.04:1

Average 11,2 St 2.01

Ghservations: Two specimens, although not

well preserved, appear to differ fram Syrio-

planarhis hardmani in having taterally eom-

pressed Whorls, which makes the shell rela-

tively higher than §. Aardmeni, with an average

dizmeter: height catio of 2.001 in contrast with

2Z37c1 average of ten specimens of 8. Aard-

mani, eis not known whether the three spiral

nibs visible on the internal east persist as ex-

lernal feaiures.

There are not sufficient specimens. nor ate

they well enough preserved, to warrant a new

specific name.

Distribution: Locality 6138 RS 87, 4 km N of

“Billa Kalina”, BILLA KALINA |-250 000

map sheet.

Habitat; Freshwater,

Genus PHYSASTRA Tapparone-Canetri,

(883

Physastra rodingae McMichacl

FIG, 3x

fsidara, near ft. peetorosa, Etheriige in

Cameron 1901; I4

Bullinus sp. nov. Chapman 19372 63

fsodora (sic), Whitehouse 1940724

Physavtra rodingae McMichael, 1968: 146, pl.

11, figs 2-5

Material, Four poorly-preseryed casts and

moulds, mostly enthedded in hard limestone,

GSSA M3581 (14), loculity 6238 RS 87, 4

km N oof “Billa Kalina’, They appear to he

casts and external moulds of juveniles, with

about 3 whorls, of the sinistral species whieh

has 4-5 whorls in the adull,

M3581(1), an internal cast freed from the

matrix, has dimensions: height 9.0, diameter

5.3 mm, compared with a height 33.0+, dia-

meter 14.5 mm in the largest paratype.

Type lacality; NT 407, 12 km NE of “Deep

Well", 66 km SSE of Alice Springs, RODINGA

1:250 000 map sheet, Unnamed formation,

Distribution: Western Austealia-White Moun-

tain Hills, White Mountain Formation, 15 km

—B of NS of “New Ord River’, LISSADELL

1.250000 map sheet; Northern Terntory —

NT 407, unnamed formation, 12 km NE of

“Deep Weill", ROPINGA 1;250000 map

sheet; NT 424, Waite Formation. 6.4 km § of

“Alcoota” H,S,, ALCOOTA 1:250000 map

sheet; Queensland—-Q1!, Carl Creek Lime-

stone, & km N of “Riversleigh” H.S., locality

103 on LAWN HILL 1:125 000 map sheet;

QI2, Carl Creek Limestone, 1.6 kro SE of

“Riversleigh” H.S., locality 90 on CAMOO-

WEAL, 1;250000 map sheet; South Australia

— jocality 6138 RS 87, Unnamed formation,

4 km WN of “Billa Kalina” H.S,, BILLA

KALINA [-250000 map sheet, The genus

Physastra is eecatded as living in Indonesia,

Australia, New Zealand and New Caledonia.

Habitat: Freshwater,

Observation. McMichael included in the syn-

onymy Isidera, near 1, pectoresa identified by

R, Etheridye jr, cited by Caumerou (1901) and

by Whitehouse (1940) as being abundant, of

ten in crowded masses, 1n what 1s Now Known

as the Carl Creek Limestone, which overlies

Cambrian limestone near “Riversleigh" from

which Lloyd's material also caine. This syn-

omymy is accepted in the absence of any

material evidence to the contrary,

Order STYLOMMATOPHORA

Superfamily BULIMULACEA

Family BULIMULIDAB

Genus BOTHRIFMBRYON Pilsbry, 1894

Bothriembryon praccursor McMichacl

FIGS 3 a-e

Bothriembryon praccursor McMichael, 1968: 149,

pl, i, figs 7-9

Material: 34 internal casts and several exter-

nal moulds in matrix GSSA M2738 (1-5),

M2739 (1-14), M2744 (1-3), M3582 (1-4),

all from the type section, Etadunna Forma-

tion, dolomitic limestone member 2e. Lake

Palankarinna, §, Aust, (locality 68540 RS 39,

KOPPERAMANNA |:250000 map sheet).

The species is common in dolomitie lime-

stone near the base of the Etadunna Forma-

99 N. H, LIIDBROOK

tion and is here fedeseribed from internal casts

of adult specimens collected from the type

section,

Description; Shell not known, byt from the

appearance of the casis probably fairly thick,

size moderate for the genus, clongate-turbini-

form, with a moderately high spire and large

last whorl: aperture about equal in height to

spire; whorls 5, regularly increasing. Proto-

conth small but fairly high, of two whorls

With Lip immersed, adult whorls 3, slightly to

moderately inflated, suture conspicuous, Im-

bricating, Aperture subovate, outer lip gently

ufeuate, attached less than 4 way towards

adapical suture, parictal lip probably concave,

columellar lip nearly vertical, basal lip ur-

cuate; umbilical chink present. Sculpture, as

shown on internal cast, of axial [olds of

growth ridges fairly evenly spaced, about 17

on jast whorls in oblique light, some speci-

mens appear to have 2 or 3 faint and shalliw

spiral grooves on last whurl, suggesting that

there Inay be some spiral sculpture as well,

Dimensions of Jargest specimen GSSA

M2738(1) heighe 30.5, diameter 17,7 mm,

ratio height: diameter 1.72:1, average of 23

specimens height 22.4, diameter 13,5 mm,

ratio height: diameter |.66:1. Two specimens

M2738(2) and M2739¢1) are conspicunysty

narrower than «Verage, with dimensions —

M2738(2) height 25.1, diameter 14.0 mm,

ratio height: dtimeter |.80;1, M2739(1)

height 28.4, diameter 14.5 mm, fatio height:

diameter 1.96: L-.

Type localiry: Rd 21. 6 km ENE of “Deep

Well” HS., RODINGA 1:250.00) map sheet,

unnamed formation,

Distribution, Northern Territory — NT 409,

unnamed formation, 16 km NNE of “Deep

Well" H.S. 61 kun SSE of Alice Springs, RO-

DINGA 1:250 000 mip sheet; Rd 21 unnamed

formation, 6 km ENE of “Deep Well” H.S.,

RODINGA 17250000 mip sheet; South Aus-

tralia — locality 64540 RS 59, Etadunona For-

mation, Lake Palaskarinna, south of Couper

Creek, KOPPERAMANNA 1:250000 inap

sheet.

The pulmonate land snail Hothelernfevenr is

testricted to Australia, mainly che south west.

but there are represeritatives in Cerra) Aus-

tralia and Tasmania, Bethriembrvon barrett

Iredale ws commonly ound im great Qunmbers

winder bushes in coastal areas of the Nullarbor

Plain, where it survives under dry vonditious.

Habitat: Wis ikely that B, praecursor lived in

a similar enyvironinent.

Observations: MeMichael (1968) distinguished

between B. praecursor und the living B. bar-

rerli, and also the Tasmanian fossil species B,

gunnil (Sowerby), The present study supports

separating these species. The Pleistocene to

Holocene B, harretti is a larger and narrower

shell, of 173 specimens measured from Point

Sinclair, South Australia (Ludbrook 1978),

the largest was 79 mm high and 21 mm in dia-

meter, and the average 31.5 mm high, 17.7

mim in diameter, ratio height: diameter 1.78:1-

Bothriembryon guanii (Sowerby) has been

referred to in the literature as follows:

Bulinas gunnii G, B. Sowerby, 1845, in Strze-

lecki: 298, pl, 19, fig, 6 (not fig, 5}

Bullies gunnit Sowerby, Etheridge 1878; 177,

Johnston 1880: 90. Johnston L&88: 283, pl.

44, fiy, 7

Clparas guint Cunjustified emendation} G. B.

Shy sp. Harris 1897: 3

The specific name has also been attached

to @ living Tasmaniat species thought by some

authvrs to be identical with it:

Suthrieniirven gunnli var, brachysoma Pils

bry, 1900: 18, pl. 3, fig. 53

Beitriembrvin panna! Sowerby. May 1921-92;

1925: pl, 42, fig, 7

This is the speeies referred to in Iredale

(1937; 313) and May revised Macpherson

(1958, pl. 42. fiz. 7) as Tawmdnembryon tas-

manicus Pfeiffer,

Bothriembryon gunni is now represented

solely by the holotype in the British Museum

(Natural History), a internal cast embedded

in matrix aperture down. so thal complete

description is impossible. "The specimen

figured hy Johnston (1888) cannot at present

be found, and no other specimens are known.

Johnston's figure is of an clongate-turbiniform

shell with axial tibs and impressed sutures.

Although both Rulinus and Bulimus have been

widely used for genera in different families, it

may be assumed that in replacing Bulinus (a

sinistral shell, family Planorbidae) by Bulinus

Bulinns gin iv the Bulimulidae, as did alsa

OG. FF blarris tt placing the holatype in Liparis

fa synonyviy of Bothriembryan), lohnston's

figire immediately invites comparison of

Aiclimus gunniit with Tasmanembryon tasmani-

cum (Pfcitfer), recorded as common on the

vast coast of ‘Tasmania, near the sea On trees

MIOCENE NON-MARINE MOLLUSCS oi

and rocks, but the extreme paucity af material

is a barrier to confirming the identity of the

fossil.

Bulimus guant was desctibed with Nelix

rasmmanlensis Erom travertine limestune quar-

ried near Hobart Town (Strzclecki 1845),

There is some uncertainty whether this was the

quarry visited by Darwin (Banks 1970) or

that at Geilston Bay, Neither quarry ig now

accessible, That in Hobart was iclentified by

Johnston and by Banks as at the western end

om Burnett Sctreet. Johnston's figured speci-

men, occurring alsa with “Helly tasmenierivis

came (rom the Geilston Travertine which was

quarricd at Geilston Bay on the northeast side

of the River Derwent 3 km north of the Tas-

man Bridge. Johnston considered this te he

the locality visited by Darwin and by Strae-

lecki, There seems to be no way of recallect-

ing the material or of confitming that the holo-

type of Bulinus gunnii did in fact come Irom

the Burnett Street quarry and net fram Geil-

ston Bay, but Geilstoy Bay secms the more

Ikely locality, In describing the lwo quarries,

MeCormick (1847) slated Uhat he Found no

traces of shells in the Hobart Town quarry, but

Hela and Bulimus Were embedded in the upper

part of the indurated limestone quarried al

Geilston Bay, Ten specimens of two species of

“Helix” from Geilston Bay were Kindly lent by

the Geology Depariment of the University of

Tasmania, but no specimens of “Aulinus” gua-

nil have been located, One of the specimens of

“Helix” lasmuaniensix, partly embedded in

matrix, is extremely like Sowerby’s holotype,

Direct comparison of Bethriembryon prac-

curser With "Bullnuy” eunnii is therefore im-

possible at present. Moreover, the stratigra-

phic position of the limestone containing

"Bullius’ gunrnil and “Helix” tasitaniensiy can

be stated only as “Tertiary” from present

knowledge, Strzelecki considered it to he of

Pliovene age. A composite section of the Ter-

liary sediments at Gerlston described hy Iahn-

ston (1888) was modified by Tedford ef al.

(1975), Johnston reconled marsupial bones

from yellow and brown maitled caleareous

elay, which, according to Tedford ef al, is in-

terbedded with the travertine, They compared

a diprotodontid from the Geilston ‘Traver-

tine with Neapeknldia from the Etadunna

Formation, of Middle Miocene age. An ap-

Parent age of 22.4 0.5 Ma was obtuined for

basalt overlying the travertine. A sample of

carbonaccons sediments collected below basalt

at Geilston Bay on the west side of the golf

links was sent by the Tasmanian Museum to

W. K, Harris, who has informed me verbally

that “the age of the microflora is ?Pliocene-

Pleistocene; it is not related to mid-Tertiary

microfloras. Widespread in Tasmania”.

ft can only be said that dating of material

fram the sequence at Geilstou Bay is confused,

and any correlation with the Etadunna For-

mation based on molluses out of the question,

Neither “Bulinus” granii nor “Helix” tasmun-

iensiy can be compared with known molluses

from the Etadunna Formation.

Superfamily HELICACEKA

Family CAMAENIDAE

Genus MERACOMELON Iredale, 1937

Meracomelou Woydi McMichael

FIGS 3 f-l

Meracomelon (loydi McMichael, 1968:

Il, figs 10-14

Material; Nine internal casts GSSA M2740-3,

M3582 (162), one external mould,

The species was desenbed by McMichael

from internal casts and so far the Etadunna

Formation has yielded only external moulds

and internal casts. Bladunna specimens are

generally smaller und higher than the holo-

type und paratypes from the Northern Terri-

tory and Queensland, They vary considerably

in their relative height:

151, pl.

GSSA Rep. Diam. Heleht Diam./Helelet

No. (mm) (mm! ralia

M2740 22,0 17,8 1.2421

M2741(1) 185 10.0 135:1

M2741(2) 12.0 6.4 1.8751

M2742(1) 140 10.4 1,342]

M2742(2) 13,5 8.6 L.S7:1

M2742(3) 19 77 1.54;1

M2743 12.0 9.0 133:1

M3S582(1) 13.5 K.7 W553)

M4582 13.3 7,0 1.9021

Average of 9

specimens 14.2 9.5 1.49:

Average of

holotype and §

paratypes 18,9 14.0 1.3521

Type locality; NT 409, 16 km NNE of "Deep

Well’; 6) km SSE of Alice Springs, RO-

DINGA 1:250000 map sheet, unnamed for-

mation,

Divtribulion; Northern Territory — NT 409,

If km NNE of "Deep Well”, NT 407, 12 km

NE of “Deep Well”, NT 408, 1.6 km N of NT

407, and Rd 21,6 km ENE of “Deep Well”, all

unnamed formation, RODINGA 1;250000

map sheet; South Australia — locality 6450

RS 59, Etadunna Formation, Lake Palan-

yd N. H. LUDBROOK

karinna, south of Cooper Creek, KOPPEKA-

MANNA 1:250 000 map sheet.

Acknowledgments

1 am indebted to Dr R, H. Tedford (Ameri-

can Museum of Natural History), and Messrs

Richard Flint, Greg Ambrose, Alistair Crooks

and Mrs Susan Daly (Geological Survey of

South Australia) tor providing both the speci-

tens used in the study and the geological de-

tails of the strata in which they occur, Dr M- R-

Banks (University of Tasmania) provided

valuable assistance in identifying the localities

from which the latd snails were collected in

Hobart and arranged for the loan of speci-

mens, The maps and sections were drawn in

the Drafting and Survey Branch, and assistafice

with photography given by the Biostratigraphy

Division, South Australian Department of

Mines and Energy, The paper is published with

the permission of the Director-General of

Mines and Energy.

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Piavrorp, P. E,, Core, R, N. Cocknain, A. E.,

Low, GL HL & Lowry, D.C. (1975) Phanero-

zoic, Ord Basin, 4 Geology of Western Austra

lia. Mem. geal. Serv. W, Aust. 2, pp. 395-9,

Streton, R. A, Trororp, R. H. & Mraver, A. H,

(1961) Cenozoic stratigraphy and verjebrate

palacontology of the Tirari Desert, South Aus-

tralia. Ree. S. fast, Mus. 14, 19-61.

STRZELECKI, P. E de (1845) “Physical description

uf New South Wales and Van Diemen’s Land,"

(Longman. Brown, Green & Longmans: Lon-

don), Australiana Facsimile Editions No. 19.

(Libraries Board af South Australia: Adelaide).

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gica della Nuova Guinea e delle Isole adiucenti,

|, Molluschi estramurini, Ayn, Mir, Cn. Spar,

aut, Genova VW, 4-313, taf I-31) (original not

seen),

Tebrory, R. M.. Banks, M2 R, Kemp, N. R,

McDouaat, ( & Sutueriann, F. L- (1975)

Recognilion of (he oldest known foss|| marsu-

pials from Australian. Nareee 255, 14)-142.

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A3, pls, i-xiii-

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geological history of Ouecensland, 2, Tate Ter

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VOL. 104, NUMBERS 5 & 6 28 NOVEMBER, 1980

TRANSACTIONS OF THE

ROYAL SOCIETY

OF SOUTH AUSTRALIA

INCORPORATED

CONTENTS

Robinson, A. C. Notes on the mammals and reptiles of Pearson, Dorothee and

Greenly Islands, South Australia - - - - - - 95

Williams, D. L. G. Catalogue of Fivsiecen® Setirbrabs fossils and sites in South

Australia — - - - ~ - - - 101

Moore, P. S. Stratigraphy and depositional environments of the Billy Creek

Formation (Cambrian), east of the Flinders Ranges, South

Australia - ~ - - - - - - - ee ET,

Koste, W. & Shiel, R. J. New Rotifera from Australia —- - - - =. 133

McNamara, K. J. Heteromorph ammonites from the Albian of South Australia- 145

Barton, C. E. & McElhinny, M. W. Ages and ashes in lake floor sediment cores

from Valley Lake, Mt Gambier, South Australia — - = - 161

von der Borch, C. C., Bada, J. L. & Schwebel, D. L. Amino acid racemization

dating of Late Quaternary strandline events of the coastal plain

sequence near Robe, southeastern South Australia - - ~ 167

Glaessner, M. F. New Cretaceous and Tertiary crabs (Genitaces: Brachyura)

from Australia and New Zealand - - - - - 171

van Beurden, E. & McDonald, K..R. A new species of C jd a (Agpra:

Hylidae) from northern Queensland - = 193

Jago, J. B. & Youngs, B. C. Early tS Be pineiNiS —_ Mi SEES vane,

South Australia - - - 197

Fitzgerald, M. J. Muckera and Millbillillie—Australian achondritic meteorites - 201

PUBLISHED AND SOLD AT THE SOCIETY’S ROOMS

STATE LIBRARY BUILDING

NORTH TERRACE, ADELAIDE, S.A. 5000

NOTES ON THE MAMMALS AND REPTILES OF PEARSON, DOROTHEE

AND GREENLY ISLANDS, SOUTH AUSTRALIA

BY A. C. ROBINSON

Summary

Collections and observations of the mammals and reptiles of Pearson, Dorothee and Greenly Islands

off the west coast of Eyre Peninsula were made in November 1975 and 1976. Southern Bush Rats

on Pearson Island are smaller, breed earlier, and occur at a lower population density than on

Greenly Island. The difference in population density may be explained by the different stages in the

reproductive cycle on the two islands in November. Population estimates of the Pearson Island

Rock Wallaby and the introduced population of Tammar Wallabies on Greenly Island are given. An

annotated list of all reptiles recorded from the islands is given.

NOTES ON THE MAMMALS AND REPTILES OF PEARSON, DOROTHEE

AND GREENLY ISLANDS, SOUTH AUSTRALIA

by A. C. Ropinson*

Summary

Rosson, Ao C, (1980) Notes on the Mammals and reptiles of Pearson, Dorothee and

Greenly Islands, South Australia, Trans. R. See. 8, Aust, W4(5), 93-99, 28 November, I9KO

Collections and observations of (he mammals and reptiles of Pearson, Dorothee and

Greenly tslands off the west coast of Eyre Peninsula. were made in November 1975 and 1976.

Southern Bush Rats on Pearson Island ure smaller, breed earlier and occur al a lower popula-

lion density than on Greenly Island. The diflerence in population density may be expliined

hy the different stages in the reproductive cycle on the two islands in November. Population

celimates of the Peurson Island Rock Wallaby and the introduced population of Tammar

Wallabies on Greenly Island wre given, An annotated list of all reptiles recorded from. |he

islands is given,

Introduction

In November 1976, a biological survey of

Pearson [sland and Dorothee Island (Investi-

gator Group) and Greenly Island was under-

taken by A, C. Robinson, T, J, Fatchen, A.

Spiers and J, B. Cox (South Austrahan

National Parks and Wildlife Service) and 8, A,

Parker and W. Zeidler (South Australian

Museum).

Pearson Island is located at 34°48, 134°

176, Borothee tsland at 34°0'S, 134°15°E

and Greenly Island at 34°39'S, 134°45'E. Four

days and nights were spent on Pearson Island,

a day and u night on Dorethee Island and

four days and nights on Greenly Island. In

November 1975 a two day trip to Pearson

fsland was made and some small mammal

trapping and observation of the rock wallaby

population was carried out,

This paper presents observations made on

the mammals and reptiles of these islands. The

birds are discussed in Parker & Cox (1978)

while the yegetation wil] be examined in

Fatchen (in prep.). Previous observations

(Summarised here) are available from eXpedi-

tions to Pearson Island in 1914, 1922, 1923

(Proctor 1923, Wood-Joncs 1922, 1923,

1924), 1960. 1968, 1969 (Thomas & Delroy

1971) 1969 (Smyth 1971). 1973 (Gepp

19733), 1974 (Schmitt L975) and Field

Naturalists’ Society Mammal Club unpublished

* National Parks & Wildlife Service, Box 1782,

G.P.0.. Adelaide, South Australia S001,

L Ciepp, B. (1973) The Social Organisation of the

Pearson Island Rock Wallaby (Perragale peni-

cillata pearson’). B.Sc. Hons. thesis. Zoology

Department, University of Adelaide,

observation, from Dorcthee Island im 1969

(Smyth 1971); and from Greenly [sland in

1947 (Finlayson 1948a, b; Mitchell & Behrndt

1949),

The three islands are all essentially granite

based islands with very little of their original

limestone capping remaining, the geomorpho-

logy of Pearson and Dorothee Islands having

been described hy Twidale (1971). Mitchell &

Behrndt (1949) gave a general description of

Greenly Island, while the geology of the

Greenly Island basement rock ix described by

Webb & Thomson (1977).

The vegetation of the three islands is similar,

that of Pearson and Dorothee Islands being

deseribed by Osborn (1923), Specht (1969)

and Symon (1971) while that of Greenly was

described by Fintayson (1948. a, b), Mitchell

& Behrndt (1949) and Cleland (1950).

In addition ta the general biological survey

catricd out on the islands an attempt was

made to determine the effect of fire on the flora

and fauna. An extensive area on the southern

part of the main Pearson Island was burnt in

a fire which is belicved to have started from a

lightning strike on the island peak jin early

April, 1975 (D. Steen pers. comm.). This fire

must have been extremely hot, and total de-

struction of the above ground parts of the

vegetation has occurred over large arcas, The

extent of the fire is shown in Fig. 1.

On Greenly Island a number of fires were

lit by tuna fishermen on @ February, 1974.

The wreas burnt are shown on Fig, 2 from

unpublished records of the fire, prepared by

members of the N.P.A&W.S. who visited the

island on 24 February, 1974,

o4 A, ©, ROBINSON

Fig, 1. Pearson Island showing location of trap-

ping areas, transect courts and walluhy

populations.

Methods

An arbitrary grid system with 250 m grid

intervals Was established over the three islands

to be sampled (Figs 1, 2), Collecting and

observation efforts sampled as many of the

grid intersections as possible to obtain good

coverage of the range of habitats on the

islands. Line transects at night using a spot-

light were walked on both central and south

Pearson, and during the day on Greenly Island

to try and estimate the wallaby populations.

Small mammals were sampled by systematic

trapping using Elliot and Sherman aluminium

box traps set either on a grid pattern or in

lines. All Rattus /uscipes trapped were

weighed and individually marked by toe. clip-

ping. The reproductive condition noted by

recording if testes were descended or un-

descended in males and if vaginae were per-

forate or imperforate and if nipples were

enlarged by suckling in females.

(a) Pearson Island: On 2 November, 1975,

two traplilves were set above the northern

bay (Fig. 1). Each had 10 sites at 20 m

intervals with three traps per site. On 24—

25 November, 1976, two traplines were

set on the centre section (Fig, 1). Back

had 12 sites at 20 m intervals with two

traps per site, At the same time a grid was

established on the main island with 80

sites at 25 m intervals and two traps

per site. This grid was positioned to

sample as wide a range of vegetation ax

possible from the low Afriplex shrubland

near the coast through the closed Mela-

leuca halmaturorum scrub along the creek

and into the low Casuarina woodland on

the slopes of the island peak, In addi:

tion the grid sampled as equally as

possible areas burnt in the 1975 fire and

unburnt areas. There were 34 sites in the

burnt area and 46 unburnt sites.

Derothee Island: On 27 November, 1976,

two traplines were set in a WNW and

SE direction from the conservation park

sign on the central eastern shore, Each

had 20 sites at 20 m intervals with two

traps per site.

(b)

Greenly Island; On 29=30 November,

1976, a trapline was sel above the

anchorage (Fig, 2,), It had 12 sites at 20

m intervals with two traps per site, and a

grid was established on the northern

slopes of the main island (Pig, 3) with

48 sites al 25 m intervals and two traps

per site, This grid was positioned to

sample as wide a range of vegetation as

possible from the Pow tussock grassland

on the lower slopes to the low Casuarina

woodland on the upper parts of the island.

The grid sampled areas of grassland burnt

in the 1974 fires. It was not possible to

distinguish boundaries between burnt and

and unburnt sites due to the degree of

regeneration,

All species of mammats and reptiles re-

corded from the islands are discussed. South

Australian Museum registration numbers are

recorded of specimens collected,

MAMMALS & REPTILES OF PEARSON, DOROTHEE & GREENLY ISLANDS 95

Anthon:

Peninsula

\Wandra

Point

_ Nor'West

Crevasse

a! be West rH + ~ Fes depbensyery 6* ber ard |

Peak tm t

a8 . imsppecl 24 Fret oT

Comservatvon park Sryr |_|

1°] 400 meres

| J

a — + { —— _

ae ae

Tragptinas. iret rect

Wallaby Pour? nensents om

“Eagle de |

Poak

Varn

The Cauldron

yeecwean Mil

MAIN

| ISLAND

_ + 4

yomA

—— abe

Pe eter —

Fipute 2, Greenly Island showing location of trapping areas and wallaby count transects.

Results

MAMMALS

Family MACROPODIDAE

Petrogale lateralis Gould. Pearson Island

Rock Wallaby. This species was collected in

1920 by Wood Jones from Pearson Island

and Thomas (1922) described it as a new

species (P. pearsoni). Since then there has

been considerable confusion about its relation-

ship with other rock wallabies and this is dis-

cussed by Thomas & Delroy (1971). Recent

chromosome and electrophoretic studies (G,

Sharman pers. comm,), place the Pearson

Island animals with western and central! Aus-

tralian populations of FP. lateralis (Poole,

1979). P. lateralis also occurred in the far

north-west of the South Australian mainland

but may now be extinct. Early visitors to

Pearson Island mentioned that the rock walla-

bies occurred only on the northern section

(Wood Jones 1923), This section is separated

from the central and southern section by a

sand spit that dries at low tide, The 1960

expedition also noted the absence of wallabies

on the middle and south sections of the island

and they found no trace of skeletons or of

occupation of several caves on the southern

section. On the 1960 expedition several wal-

jabies Were caught on the northern section and

transferred to a camp on the middle section.

Four females, one male and one animal of un-

known sex escaped. It appears certain that the

present rock Wallaby population on the middle

and southern sections of Pearson Island is

descended from these six escapees.

Thomas & Delroy (1971) estimated that

there were 50-150 wallabies on the middle and

southern sections in 1968 and showed that this

1960-1968 population increase was theoreti-

cally possible from the original six animals, In

1976, transect counts of the middle section

in the evening (24 November) and at night

by spotlight (25 November) revealed 64 and

40 individuals respectively, while a spotlight

transect on the southern section (25 Novem-

ber) revealed 92 individuals. Thus the total

population of the middle and southern sections

is at least 150, The distribution of this popu-

lation is shown in Fig. 1.

on A, C. ROBINSON

{t is much more difficult to estimate the

wallaby population on the northern section of

Pearson Island. The population ts fragmented

(Fig. 1) being confined to areas with suitable

rook crevices and caves and the dense veyeta-

tion makes sighting difficult. Thomas & Delroy

(1971) provide two estimates for ihe northern

section; 1960—500 to 600 and 1968 ib excess

of 500, In November 1975, the author walked

over the whole of the jorthern section and

counted 132 individuals: this was undoubtedly

too law and the total population is probably

iwice this size between 250 and 300, No

estimmles of the population on the northern

section were uttemped in 1976,

The diet of the wallabies was observed to

include Lepidinm faliosum, Atriplex ¢inerea,

A, palidosa, Rhagedia baccata, Enchylaena

tomentosa, Olearia runiulova, Carpohratas

rossii ind Disphyma australe. Og the parthern

section, even around the major colonics of

wallabies there was lime evidence of grazing

of the vegetation. On the middle and southern

sections however, large areas of vegetation

were obviously very heavily grazed. This was

particularly the case with E turmentose, while

D. australe and A, paludosa were also being

affected.

Macropus cugenii (Desmarest) Tammae,

SAM, M9786, An unknown number of Tam-

mars were introdiiced to Greenly Island frarn

Kangaroo Island in about 1905 to act as an

emergency food supply for possible castaways

(Mitchell & Behrndt 1949). They now occur

an both the main central und small south-

Western section of the island but are apparently

absent from the northern section. They spend

the daytime tn the dense teatree thickets on

the south side of the main ridge Of the istund

and also occupy some of the gullies on the

northern slopes of the island, They are ex-

tremely difficult to observe aud the two transect

counts (Fig. 2) resulted in the sighting of

four and 14 individuals, Il is proheble that

the total population is about SQ individuals.

The stability of (he Tammar population on

Greenly Island is hot knowl, bul a eormpari-

son Of the Vegetation of the main island with

the northern section where wallalles are absent

reveals that they have had a sabstantial |mpact

on the island vegetation, Phere his heen signi-

ficant reductions in both species diversity and

ground cover and ih appears that the present

veneration of ihe main section of Creenty

Islan! is a direct result of severe ovet-grazing

by the introduced Tammar population over the

last 70 years.

Family MURiDAE

Ralins Juscipes (Waterhouse). Southern

Bush Rat SAM M9787-91, This species is

comma on both Greenly and Pearson Islands

ful appears absent From Dorothee Island, The

pupulations on both islands Were probably

derived from a population distributed across

most of Southern Australia during the last

ice age When both the islands were connected

to the mainland, Sehmitt (1978) and Schmitt

& White (1979) haVe estimated thal Pearson

and Greenly Islands have been isolated from

the mainland for 14000 years. They have

emphasised the importance of genetic drift

in producing the differences between the island

populations that they studied. The grid trap-

ping carried out on this expedition provides

an opporiunity to obtain additional compara-

tive data, Accordingly, the two islands are

discussed separately below,

Pearson Island

Schmitt (1975) has demonstrated that sig-

nificant genetic differences occur between the

Bush Rat populations on the northern and

southern sections of the island, The grid was

located on the northern section (Fig, 1) and

the following discussion refers to this popula»

fion only,

(a) Pepulation density: Twenty-six individuals

were captured on the 50000 m* of the

grid, Therefore, ignoring boundary effects,

the overall density was 5,2 rats/ha.

As approximately half the grid was in

the area burnt by the 1975 fire it is appra-

priate to examine the differences in popu-

jallon density i the burnt and unburne

areas: Burnt sites 3.8 rats/ha; unburne

sites 6,3 rats/ha.

{b) Ser ratio 1% dc + 13 29

9? 49.1 gy (30-70, n = 13)

Reproductive status: All the males cap-

tured were sub-adult with undescended

testes. Five of the females still had im-

perforate yaginas while those with per-

forale vaginac showed no indication that

their nipples had been suckled, This sug-

gests that there had been a spring breed-

ing season with a very high mortality of

(dd)

MAMMALS & REPTILES OF PEARSON, DOROTHEE & GREENLY ISLANDS 97

both male and female adults to result in

this largely immature population im

November.

Greenly Island

Although the part of the island covered by

the trapping grid had been burnt in 1974, it

was impossible to distinguish burnt and un-

burnt areas, so the whole grid was treated

as a single area.

(a) Population density: Thirty-seven in-

dividuals were captured on the 30 000 m*

of the grid, Therefore, ignoring boun-

dary effects the overall density was 14.3

rats/ha,

(b) Sex ratio: 18 des 19 99

18); 22 70.7 g (40-100, n — 19)

Reproduetive status: Seven of the males

were sub-adult but although all the re-

maining males were of adult weight, only

two still had descended testes, OF the

females three still had imperforate vaginae

while four of those with perforate vaginae

had developed nipples, indicating a recent

cessation of the feeding of the young.

This suggests that the breeding season

had just ended and that at this stage in

the population cycle there had heen a high

survival of both males and females from

the parental generation.

A comparison of the Bush Rat populations

of Pearson and Greenly Island indicates that

the Greenly Island population occurs al a

significantly higher density, even considering

the population density on the unburnt portion

(d)

of the Pearson Island afid, In addition the

Greenly Island animals were much heayier

and larger than the Pearson Island animals.

Finally it appears that at least in 1976 there

was a spring breeding season with a possibility

of breeding continuing into early November

on Greenly Island.

Additional comparative data on Bush Rat

population densities oa South Australian off-

shore islands are shown in Tuble 1. The figures

are given as trapping percentages and with

the exception of this present study are based

on (rap lines rather than grid trapping so no

absolute densities can be obtained.

The differences in population densities be-

tween Pearson and Greenly Islands shown

by the grid studies are also apparent in the

line trapping. Schmitt's line trapping figures

obtained in February and March however

showed similar trapping success rates oa hoth

islands and it is possible that the differences

demonstrated in the grid study in November

may be due simply to greater survival of adults

from the breeding season on Greenly Island

than on Pearson Island, The high trapping

success on other South Australian offshore

islands indicates that high population densities

of Bush Rats are a feature common to all

of these islands,

Family OTARIIDAE

Neophoca cinerea (Peron & Lesueur) Aus

tralian Sealion. This species was present on

each of the islands visited.

Pearson island: 20-30 individuals, 4-6 mature

bulls, the major concentration wis On the

beach on the centre section of the island

TABLe 1. Comparison of results of irapping studies of Rattus luscipes en South Australian offshore

ishirils

Trapping

Type of Success

Island Month Trapping 5a Source

Narth Pearson [. Noy line 5 This Study

North Pearson [. Feb line Ai} Schmitt (pers. commt.)

North Pearson I. Nov erid 8 This Study

South Pearson 1, Feb line i Schmitt (pers, comm.)

South Pearson I, wav line 19 This Study

Greenly }. Mar line 22 Schmult (pers, comm),

Greenly I. Nov line su This Study

Greenly 1. Nov grid 21 This Study

Waldegrave L. Feb line 68 Schmitt (pers. comm.)

Williams I Apr line $2 Schmili (pers, comm.)

North Gambier 1. Apr Tine 52 Schmitt (pers. conim.)

Dog I. Jun line 73 Schmitt (pers, comm.)

Goat |, Jun line 62 Schmitt (pers. comm. }

ee __. Ee

98 A. C. ROBINSON

Dorothee Island: 30 individuals, 7 mature

bulls, the major concentration was on a sloping

tock shelf on the north side of the central cre-

vasse and on the saltbush covered slopes

around a wallowing area.

Greenly Island: 30 individuals, 4 mature bulls,

the major concentration was on a sloping

granite shelf on the north face of the main

island.

On all islands there were immature animals

1.5-2 m long associated with females, and

some were observed to be suckling although

they were often abandoned by their mothers

on the higher parts of the island.

Arctocephalus forsteri (Lesson). New Zea-

land Fur Seal. This species was found only on

Dorothee and Greenly Islands.

Dorothee Island: 16 individuals, 1 mature bull,

concentrated in cracks and holes in the rock

around the central crevasse.

Greenly Island: 40 individuals, 4 mature bulls

with the major concentration on the sloping

granite shelf on the north face of the main

island near the blowhole. There was another

small group in the south crevasse.

On both islands there were some immature

animals 1-1.5 m long still associated with their

mothers.

REPTILES

Family GEKKONIDAE

Phyllodactylus marmoratus (Gray). Mar-

bled Gecko SAM, R15800A-—D, R15802, A,

B, R15807 A-D, R15809, R15815 A, B.

Previously reported by Proctor (1923),

Mitchell & Behrndt (1949) and Smyth (1971).

Found on all three islands. Common in areas

of limestone capping but also under exfoliat-

ing slabs of granite. Two clutches of eggs

found on Pearson Island under a large slab

of granite contained 14 and six eggs respec-

tively. As this species lays only two eggs at a

time it would appear that communal laying

occurred at favoured sites.

Underwoodisaurus millii (Borg). Although

not recorded in his paper, Smyth deposited

specimens of this species from Pearson Island

in the S.A. Museum. (R10237 A—B).

Family PyGoropIDAE

Aprasia striolata (Lutken), Although not

recorded in his paper, Smyth deposited a speci-

men of this species from Pearson Island in the

S.A. Museum. (R10232).

Family AGAMIDAE

Amphibolurus fionni Proctor. Peninsula

Dragon SAM R15801, R15803-6, R15820

A-B. Only found on Pearson and Dorothee

Islands and previously reported by Proctor

(1923) and Smyth (1971). Closely associated

with granite out-crops. Further details of its

offshore island distribution are discussed by

Houston (1974).

Family ScrincipAE

Egernia multiscutata Mitchell & Behrndt

SAM R15182 A-B, R15813 A-—B, R15814.

Recorded only from Greenly Island (Mitchell

& Behrndt 1949). It was recorded only from

Greenly Island on this occasion and found

to be abundant in the Casuarina woodland,

living in burrows beneath fallen logs and rocks.

Also trapped in the Poa _ grassland but

appeared much less common in this habitat.

Hemiergis peronii (Fitzinger) SAM R15808

A-C, R15810 A-—B, R15811 A-B, R15816 A,

B. Found on all three islands, previously re-

ported by Proctor (1923), Mitchell & Behrndt

(1949) and Smyth (1971). It was common in

loose soil and accumulated organic matter at

the base of plants and under rocks and fallen

timber.

Leiolopisma_ entrecasteauxii (Duméril &

Bibron). A single specimen was collected from

Pearson Island in 1923 (Proctor 1923). It has

not been collected there since.

Lerista frosti (Zietz). Not found by the

present expedition but reported to be common

on Pearson and Dorothee Island (Smyth

1971), while a single specimen (recorded as

Rhodona tetradactyla) was taken from the peak

of the main section of Greenly Island (Mitchell

& Behrndt 1949).

Lerista picturata’ (Fry). Although not

recorded in his paper, Smyth deposited a speci-

men of this species from Pearson Island in the

S.A. Museum (R10235).

Menetia greyii (Gray). Recorded on Green-

ly Island by Mitchell & Behrndt (1949) but

not seen or collected in 1976,

Morethia obscura (Storr). SAM R15819.

Small fast moving skinks probably of this

species were seen on Greenly Island and one

specimen was collected from Pearson Island.

It has been recorded from Pearson (Smyth

1971) and Greenly Islands (Mitchell &

Behrndt 1949), as M. lineoocellata, but not

from Dorothee Island.

MAMMALS & REPTILES OF PEARSON, DOROTHER. & GREENLY ISLANDS 9

References

Criecanp, J. B. (1950) Patina and Flora of the

Greenly Islands. Part 11 Flora. Rec. S. Aust.

Mus, 9, 349-351.

Fintayson, H. H. (1948a) Greenly Island, South

Australia. §, Aust. Orn. 18, 72-73.

(1948b) Greenly Island, South Australia.

Walkabout. 14, 35-38.

Houston, T. F. (1974) Revision of the Amphi-

holurus decresii complex (Lacertilia: Aga-

midae) of South Australia. Trans. R. Soc. S.

Aust. 98, 49-60.

Mrrciett, F. J. & Benrnot, A. C. (1949)

Fauna and Flora of the Greenly Islands Part

1. Introductory narrative and yertebrate fauna.

Ree. 8S, Aust. Mus. 9, 167-179.

Osnorn, T. G. B. (1923) The Flora and Fauna

of Nuyts Archipelago and the Investigator

Group No. 8 The Ecology of Pearson Islands.

Trans, R. Sac. 8. Aust. 47, 97-118.

Parker, S. A. & Cox, J. B. (1978) Notes on the

birds of Pearson, Dorothee and Greenly Islands,

South Australia. ibid. 102, 191-202.

Pooie, W. E. (1979) The Status of the Australian

Macropodidue. In M. J. Tyler, (Ed.) “The

Stutus of Endangered Australasian Wildlife”,

. 13-27. (Royal Zoological Society of 5.

Aust., Adelaide).

Proctor, J. B. (1923) The Flora and Fauna of

Nuyts Archipelago and the Investigator Group

No. 5—The Lizards. Trans. R. Soc. 8S. Aust.

47, 79-81.

Russett, T. C. (1973) Australia Pilot Vol, L

South Coast from Cape Leeuwin to Green

Point. 6th Ed. Hydrographer for the Navy.

Scumitr, L. H. (1975) Genetic evidence for the

existence of two scparnte populations of Rattus

fuseipes greyii on Pearson Island, South

Australia, Trans. R. Soc. S. Aust, 99, 35-38,

—— (1978) Genetic variation in isolated popula-

tions of the Australian Bush Rat Rattus fuscipes.

Evolution 32, 1-14.

& Wuire. R, J. (1979) A comparison of

metric and protein variation in the Australian

Bush Rat Rattus fuscipes greyii. Aust, J, Zool.

27, 547-559.

SmytTH, M. (1971) Pearson Island Expedition

1969-5. Reptiles. Trans. R. Soc. S, Aust. 95,

147-148.

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Tuomas, I. M. & Derroy, L. B. (1971) Pearson

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Nuyts Archipelago and the Investigator Group

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15. The Pearson Island Rat and the Flinders

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CATALOGUE OF PLEISTOCENE VERTEBRATE FOSSILS AND SITES IN

SOUTH AUSTRALIA

BY D. L. G. WILLIAMS

Summary

The Pleistocene vertebrate fossil sites of South Australia are listed, summarising fossil assemblages

and depositional environments. References to the literature are provided. A list of SAM specimens

is available.

CATALOGUE OF PLEISTOCENE VERTEBRATE FOSSILS AND SITES

IN SOUTH AUSTRALIA

by D, L. G, Witciams*

Summary

Wuaiams, D. L. G. (1980) Catalogue of Pleistocene vertebrate fossils und sites in South

Australia. Tran, KR. Sov. 8. Aust, 104(5), 101-115, 28 Novernber, 1980.

The Pleistocene vertebrate fossil sites of South Australia are listed, summarising fossil

assemblages and depositional environments. References to the literature are provided, A list

of SAM specimens is available.

Introduction

The Catalogue originated as part of a Ph.D,

research project involving Lute Pleistocene los-

sil vertebrates and palacoclimates in the Flin-

ders Ranges area of South Australia, Informa-

tion from museuni records, published work and

the author's own field observations is sum-

marised but discyssion is kept to a minimum,

Sites are listed in numerical order, based an

geographic proximity. An alphabetical index is

provided, Names contorm as far as possible to

the Australian 17250000 Gazelleer (Division

of National Mapping, Dept ef Minerals &

Energy 1975). Referred mup sheets, e.g.

ORROROO, are in the 1:250 000 series, Cave

sites dre numbered according to Lewis (1976),

Sites in the .. Eyre region are distinguished by

numbers (c.g. V5772) assigned by the UCMP,

A key to all sites is given in Figure 1.

lnstitulions housing relevant fossil collections

are abbreviated’ SAM — South Australian

Museum, FUSA—Flinders University of South

Australia, AUGM—Adelaide University Geo-

logy Museum. SADME— South Australian

Department of Mines and Energy, NMVY—

Nalional Museum of Victoria. AM—Austra-

lian Museum, AMNEL—American Museum ol

Natural History. UCMP—University of Cali-

fornia Museum of Paleontology. SI—Smiih-

sonian Institution, BMNH—British Muscum

(Natural History), UM—Hunterian Museum.

In presenting lists of previously published

assemblages, the identifications of other authors

are quoted directly, although in some cases

taxa do not conform to current usage, Pub-

lished lists are avatlable for sites 1-3, 16, 47,

48, 54, 55, 63, G41. 64e. Other assemblages

have been mentioned in the literature, bul were

not necessarily identified formally. These data

reter to sites ¥, 18, 20, 31, 40, 42, 52, 53, 5h,

* School of Biological Sciences, Flinders WUniver-

sity of South Australia, Bedford Park, S. Aust

5042.

57, 60, The majority of sites, however, are

unstudied, Much of the material has been exa-

mined by the author, but not in detail, Tdentifi-

cations rely on museum catalogues and collec-

tions, Sites involved are 4-8, 10-15, 21-24,

28, 32, 38, 41, 43, 45, 49-51, 57-59, G1. 62,

64, 46-68. The remainder of the sites full into

two categories. The first includes sites under

detailed study by the author; 17, 19, 22, 25-27,

29, 30, 33-37, 39, 40, The second includes

assemblages personally communicated by other

workers: sites 44, 46, 641, Specimen numbers

are not given here, but a list of SAM catalogue

numbers, arranged geographically, is available

from the author.

The Catalogue should not be used directly

as a source of biogeographic information, Until

more is known of the ages of the deposits, und

the bias affecting the fossil assemblages, such a

use would be premature, The Catalague is in-

tended os a summary, which will facilitate

access to museum collections, and draw atten-

tion to deposits which may have been over-

looked,

Catalowue

1. WEEKES CAVE (N15)

(COOMPANA),

Nullarbor Plain, near Koonalda Statin, SAM,

BIRDS: Threskiornithidse; Plarihus flavipes.

Accipitridae; Accipiter fasciatus.

Falconidae; Falco cenchroides.

Turnicidac; Turnix sp,

Sylviidae; Cinclorhamphus cruralis, C_ mathewst.

Estrilidae; Poephila exnata.

Artamidae; Artumus leucorlivnetus-

yan Tets (1974b).

2, CALCA 33°02'S, 134°22'E (ELLISTON)

SE of Streaky Bay, near Baird Bay. Red sandy

sediments 5-7 m deep in well excavation. SAM,

MARSUPLALS; Macropodidae; Srhenisus sp,

Pracaptodpn xolialt,

Merrilees & Ride (1965).

35°31°S, 1IYSSE

102

OVewOonf Gry —

KEY

WEEKES CAVE

CALCA

BROTHERS ISLANDS

KYANCUTTA

PANDIE PANDIE

GOYDER'S LAGOON

WARBURTON RIVER

INNAMINCKA

COOTANOORINA

LAKE KANUNKA

COOPER CREEK

LAKE PALANKARINNA

HERGOTT SPRINGS

WELCOME SPRINGS

MURNPEOWIE

LAKE CALLABONNA

BILLEROO GREEK

PERNATTY LAGOON

HOOKINA CREEK

MOUNT EYRE

WILLOCHRA CREEK

BOOLCUNDA CREEK

BUCKALOWIE CAVES

TEETULPA

DEMPSEY'S LAKE

ARNOLDS BANK

HILLPARA CREEK

NECTAR BROOK

PEKINA CREEK

BLACK ROCK GRAVEL PIT

MANUNDA CREEK

PORT P[RIE GRAVEL PIT

WAUPUNYAH CREEK

ULOOLOO

COLLINSVILLE

NEWIKIE CREEK

BALDINA CREEK

BUTE

BURRA CREEK

BUNDEY

MORGAN

CHOWILLA

CURRAMULKA

LAKE FOWLER

PONDALOWIE BAY

ROCKY RIVER

KELLY HILL. CAVES

EMU CAVE; SETON ; MT

HOG BAY RIVER

KAPUNDA

TWO WELLS

GAWLER

YATALA

FROMM’S LANDING

DEVON DOWNS

CHUCKA BEND

ADELAIDE AREA:

BROMPTON

CROYDON

FINDON

KIRKALDY PIT

THEBARTON

HALLETT COVE

ECHUNGA

YANKALILLA

SALT CREEK

Fig, 1. Distribution of Pleistocene vertebrate sites in South Australia.

—

D. L. G. WILLIAMS

South

Australia

TAYLOR

GOOLWA

BLACKFORD DRAIN

HENSCHKE’S BONE DIG usu

JAMES’ QUARRY

NARACOORTE CAVES

PENOLA

TANTANOOLA AREA:

GLENCOE

GREEN WATERHOLE

MILLICENT

MT BURR CAVE

TANTANOOLA CAVE

MOUNT GAMBIER

TANKSTAND CAVE

134

i236

PLEISTOCENE VERTEBRATE FOSSILS Ls

3. BROTHERS

(LINCOLN),

Western end of western island, in Coffin Bay

Eroded gave mined for guano for a few yeurs

from 1902. SAM.

MARSUPIALS: Macropudidae;

Sthenurus ef, maddocki,

EUTHERIANS; Otariidae; Aretocephalus sp.

KIRDS’ Dromornithidae; Genyornis newtont,

Unidentified small bird banes.

Jack (1919), Johns (1966), Rich (1979),

ISLANDS 34°35°S, 135°20E

Macropus ap,

4, KVANCUTTA 33° 08'S, 135°33°E (KRIMBA),

Central Eyre Peninsula. Bone fragments sod teeth

labelled “Kyaneutta N.S\W". Specimens possibly

collected in N.S.W., and acquired from the defunct

Kyaneutta Museum. (T. HO Rich pers, comm.

1979). NMYV,

MARSUPIALS: Diprotodontidac; Diprotndon sp,

5, PANDIE PANDIE 26°08'S, 139°23’E (PAN-

DIE PANDIB).

Foy NE. of South Australia. Ineisor and bone frug-

ments. SAM.

MARSUPLALS: Diprotodontidae; Dipretedan sp.

f. GOYDER'S LAGOON 27°0I'S, 138°54'E

(GASON),

Diumuntina River. Bone fragments. SAM,

MARSUPIALS: Diprotodontidae; ?Diprofodon

Sp.

7. WARBURTON RIVER, A number of siles be-

iween L, Eyre and the Birdsville Track. Fossils

(rom Katipiri Sands equivalent. SAM, HM,

UCMP. Note: Lists of fossil assemblages derived

from UCMP collection,

a. Cassidy Locality (V5539) 27°48'S, 138° 12'E

(GASON),

MARSUPTALS: Vombatidacy Phascolonus cf.

Rigas.

Dipratadontidae: Dipretodon sp.

Macropodidae; ?Onyelogalea sp. Pratemnadan

cl, brehas, Srhenurus ef, oecidentalin.

RIRDS: Dromorniihidue.

REPTILES: Varanidue; Mevalania sp,

bh. New Kalamuring (V7205%) 27°44'S, 138°

17°F (GASON),

MARSUPIALS:

vivas,

Diprotedontidac: Dipraradon cf, eptatum,

Muacropodidae; Macropus sp.. Sthenurus sp. Pra-

cepieden ch. raphe.

REPTILES; Varanidae; Meeulunia sp,

Crocodilians

PISH: Unidentificd material.

¢. Marens Locality (V5569) 27°53'S, [37°50 E

(NOOLYEANA)

MARSUPIALS:

laniarius

Diprotodontidae; *Zygomalurus sp,

Macropacidae.

Vormbatidae: Phascolonuy ct.

Dasyuridae; Sareaphilus — cf.

d. Greeo Biufl Loeabity (V5775) 27°53°S, 1377

36'R (NOOLYEANA),

MARSUPIALS: Vombauduer

wivas.

Dipratodontidae; Diproteden cf. oplatum, ZvKe-

mialurus sp.

Macropodidac; Matropus sp., Osphranter sp.,

?Wallabia sp., Protemnodon cf anak, Sthenurts

sp.. 5S. cf. orientally, S. cf. pales, 8. cf, rindalei,

Pracaptodon cf, goliah, P. cf. rapha.

BIRDS: Anhingiaes Anhinga sp,

Phalacrocoracidac; Phialacracorax carbo.

REPTILES: Varanidue. Mevalania sp.

Chelonians and Crocodiljans,

FISH; Siluriformes and Dipnoy.

ec, Lookout Locality (V5776) 27°52'8, 147°55 E

(NOOLYEANA),

MARSUPIALS:

gigas,

Diprotodontidue: Pipraredon cf. aptaium

Macropodidae; Mucropus sp. Sthenurus cf ander-

sont, Pracapladon ef, raph,

BIRDS; Phalacrocoracidue; Phalacrocerax varity.

REPTILES: ?Varanidae..

Chelonians and Croeadilians.

FISH; Siluriformes and Dipnoi.

F. Punkrakadarinna Soakage (V5777) 27°47'S,

137°49'E (NOOLYEANA).

MARSUPIALS: Diprotodontidae: Diprotodan cf.

aptatum.

Tate (1886), Zietz (1899), Etheridge (1894), Sti-

ling (1913). Howchin (1930), Stirton ef al.

(1961), Pledge (1973), Hecht (1975), R. H_'Ted-

ford (pers. comm. 1980).

8. INNAMINCKA 27°45'5,

MINCKA),

NE of South Australia, SAML

REPTILES: Varanidse; Megalania prisca.

9. COOTANGORINA 28°10'S, 135°18'E (WAR-

RINA).

NW of L, Eyre, near The Peake. Jaw found at

depth of “26 to 30 feet’ in well excavation, “al

the head of one of the mound springs” (Chandler

1882).

Phascolonus —cF.

Vombatidae; Phasenlenus cf.

40°44 BE (INNA-

MARSUPLALS: Diprotodontidae; Dipretodun

ansthalix.

Chandler (1882), Brown (1894), Howehin

(1930),

lia LAKE KANUNKA = 28°23'S, [38° 18'F

(KOPPERAMANNA)

Fast of L. Eyre. Kanunka Fauna in Raupin chun-

nel sands and floodplain deposits, ?Rarly Pleisto-

cence. SAM, NMY, AMNH, Si, UCMP V5772Z and

VS5773.

MARSUPTALS: Dasyuridie.

Vombatidaes Pluiscolonus sp., cf. Vembarus ar

Lasierlinus sp.

Thylacoleonidae,

Diprotodontidac, ef,

PaluUrus sp.

Diprotadan sp., ch Zypo-

104 DL. G, WILLIAMS

Macropodidac; Aetrongla sp,, Matrapus spp. Os-

phranter sp., Lagorchestes sp., cl. Wallabia sp,, ef.

Prionwtemmnus sp., Tropasodon kenili, Protentie-

don sp. Sthenurus sp,

EUTHERIANS: Muridae,

BIRDS; Dromornithidae; Genwornis sp,

Phalacrocoracidae; Phalacrocorax spp.

Anatidae; Anas sp., Cyeruy sp.

REPTILES: Varanidae,

Unidentified Chelonians and Crocod)lians.

FISH: Ceratodontidae; Epiceratodus sp.

CRUSTACEANS; Decapads.

Debney (1882), Tate (1886), Stirton ef al.

(1961), Ro H. Tedford (pers. comm. 1980),

0b, MURRAPATERINNA 28°26'S, 138°31'E

(KOPPERAMANNAI.

Between L. Kanunka and Mulka. Fossils from

bore [S m deep, 28 Avy. 1921, SAM Director.

Waite, identified Crocodilian, Lunefish, and

Macropodid teeth and bones.

Also, NMV collection Nov, 1929, “Marree via

Mulka perv Sir Colin MacKenzie” from George

Aistog;

MARSUPTALS: Diprotodontidac; Diproieden sp,.

’Zygomaturns 8p,

Mactopodidae; Macropus sp.. Protemnodon sp.

11. COOPER CREEK. A number of sites between

|. Eyre and the Birdsville Track. Katipiri Water-

hole is the type locality for the Kalipiri Sands

(FP l\o-Pleistocene) from which fossil vertebrates

ure eroded by the creek. SAM, NMV, AMNH,

UCMP, EMNH, HM, Note: Lists of fossil assem-

blages ure derived from the UCMP collection

a, Cannatalkaninna (V5377) 28°40'S, [38°26°E

(KOPPERAMANNAI!-_

East Cooper crossing, 7Sub-Recent.

MARSUPIALS: Dasyuridae.

Muridae; Rattus sp,, Notamys sp,

bh. Unkumilka Waterhole (V5378)

138°19'R (KOPPERAMANNA).

MARSUPIALS; Diprotodontidae; U/preradart sp..

*Zyeomaturns sp.

ce. V5379 28°39'S,

MANNA),

SE of While Crossing.

MARSUPIALS: Thylocoleantdac; ?Thyhicalee sp.

Diprotodontidpe; Diprofodorn sp.

Macropodidae: ?Praceptodan sp.

REPTILES: Varanidae; Megalanin sp.

28°41°S,

MB Sh (KOPPERA-

4d VS5380) 28°37'S, I38°I4E (KROPPERA

MANNA},

MARSUPIALS; Macropodidae; Macropus of.

titer.

PUTHERIANS: Muridae,

& VS38I 28°35'S, J3R°I3E (KOPPERA-

MANNA).

Near Tilla Tilla Waterhole,

MARSUPIALS: Thylacoleonidaes ?Thylacolen sp

Diprotodontidac; Dipratodon cf. aptatum,

Macropodidac; Muerepus sp,, Pretemnedan sp,

Sthenurus sp.

BIRDS: Dromo:nithidae.

f, Malkuni Waterhole (VY5382) 28°34'S, [38°

07 E (KOPPERAMANNA),

MARSUPIALS; Diprotodentidae; Dipratedon sp,

Macropodidae, Macrepus cl. titan, small Macro-

podid, Proremineden ch anak, P. cf. brehue,

Sthenurus sp., Procéptoden cf, goliah.

BIRDS: Dromornithidaec.

Phalacrocoracidae; Phalacrocorax carho, P, varius.

Tytonidae, Tyre cf, novaeliallandiae,

2 V5859 28°33'S. 138°09'E

MANNA).

MARSUPTALS: Dasyuridac; Sarcophilus sp,

Diprotodontidae; Biprotadoan cf. minor.

Macropodidaes *Procopioden sp.

BIRDS: Phalacrocoracidne: Phalacroconay sp,

REPTILES: Crocodihans.

FISH: Cermtodontidae; Epleerarodus sp.

h. VS860 28°35'S, I38°0S°R (KOPPERA-

MANNA).

MARSUPIALS: Dasytridae: Sarcophitus sp.

Vombatidae: Phascolonns cf gigas.

Phalangeridae; Vrithasvrus cf. valpecula.

Diprolodontidae; Diprotedon sp, DB, cf. minar,

?Nototherium,

Mucropodidae; Betrangia cf, lesuene, Macropus cf,

titan, Lagorchestes yp., ?Onychoyalea sp. Protern-

nodan sp. Po cf brehus, Sthenurus sp. Sy cf,

andersoni, 8, cf, brawnei, Proceptadan cf. goliah,

Pict. tapha,

EUTHERIANS: Muridae.

BIRDS; Dromornithidae,

REPTILES: Varanidaes Megalania sp.

Chelonians and Crocodilians.

i. V5861 28°54'S, 1[38°OS'F

MANWA).

Katipiri Waterhole (Cuttapirra Waterhole),

(KOPPERA-

MARSUPTALS; Vombatidac; FPhascelonuy cl

Rigas.

Diprotodontidae; Dipretadan sp,, ?Zyeornaturis

Mucropodidae; °Hallabia sp. Pretemnodun cf,

anak, Sthenuras sp.. 8. ef. rindalei, Procoptodar

ef, goliah,

BIRDS: Dromornithidae.

Anhingidae; Aniinga sp.

REPTILES: Vurunidue; Megalania xp,

Chelonians and Crocodilians.

FISH; Ceratodontidac.

j, VS866 24°34°S, 138°00'E (LAKE EYRE/

KOPPERAMANNA|,

MARSUPIALS: Vombatidae; Phascolanis sp.

Diprotedontidae; Diprotedon sy, ?Z7ygomaturnue

SP,

Macropodidac; Proaremnodon cf. bredins, Sthenuray

cf. andersoni, §, cf, rindalei, Proceprodon sp.

BIRDS: Anhingidae; Anhinga sp.

Phalactocoractdae: Phalacrocoray carbe,

Analidae; Bizivra sp.

PLEISTOCENE VERTEBRATE FOSSILS {Ns

REPTILES: Varunidae; Mezalania sp

Chelomans and Crocodilians,

FISH: Silurifarmes and Dipnoi.

k. VS5868 28°32°S, 137°59E (LAKE EYRE).

MARSUPIALS: Diprotodontidae.

Macropodidue.

BIRDS: Unidentified material,

|, V6147 28°34°S, 138°09E (LAKE EYRE),

MARSUPIALS: Thylacoleonidae: Thylacoles sp.

Diprotadontidae: Diproreden sp.

Macropodidie.

BUTHERIANS: Muridae; Ratiny sp.

BIRDS: Phalacrocoracidae: Phalacrocera. sp,

REPTILES: Varanidae; Megalaniu sp.

Crocodiliuns,

FISH: Unidentified material.

CRUSTACEANS: Decapods.

m. Unnamed focality, approx. 28"00'S, 139°30°R

UNNAMINCKA).

Far NE South Australia, near Cooper Creek.

Tooth recovered hy drilling crew, SAM,

MARSUPIALS: Dipratodontidae.

Tale (L886), Stirton et al. (1961), Rich ev al.

(1978), Rich (1979), Tedford (pers. comm.

19R0)).

12. LAKE PALANKARINNA 28°46’S, 138°25’E

(KOPPFERAMANNA!

Eust of L, Fyre,

a, Channel Sand Locality (V5854)-

Near the top of escarpment about 500 m north of

Turtle Locality. Katipiri Sands (Late Pleistocene),

incising Tirari Formation. UCMP,

MARSUPIALS: Diprotodontidae: Diprotedan sp.

Macropadidae,

Birds, Teleost fish, Chelonian and Crocadilian

remains.

b. Mullet Locality (V71173).

Sinall bluff 25 m NNW of Keane Quarry (V6265),

Katipiri Sands (Late Pleistocene) overlying Eta-

dunna Formation and overlain by Tirari Forma-

tion. FUSA, UCMP,

MARSUPTALS: Diprotodontidae; Zysomalurus.

sp.

Macropodidue; Proteninodon sp, ?Prianotemmnns

Bist

Fish and Crocodilian remains.

Slirton ef al, (1961), Rich ef al

(1979).

13, HERGOTT

IMARREE).

3 km north of Marree. Mandible, SAM.

MARSUPIALS! Diproatodontidae; Diprotedan sp.

14. WELCOME SPRINGS 29°40'S, 137°S0°E

(CURDIMURKA),

15 km SW of Marree, Hard green pebbly clay.

cemented by cileium carbonate from mound

spring. Mandible and bone fragments, SAM,

FUSA.

MARSUPIALS: Diprotodontilue: Diprofodan sp.

(1978), Rich

SPRINGS 29°37'S, 138°04E

15. MURNPEOWIE 29°35'S, 139°07'E

(MARREE).

[00 km east of Murree. Mandible, SAM.

MARSUPIALS: Diprotadonudae: Diprotoden sp.

16. LAKE CALLABONNA 79°50°S. 140° LOE

(CALLABONNA).

NE South Australia. Gypsiferous lacustrine clays

und sands, Millyera Formation. SAM, AMNH,

UCMP, SL

MARSUPIALS: Vombatidse; Phascolonnus gigas,

Diprotodontidae; Diproredon sppt?).

Macropodidae, Macrepus spp., Protemnodan sp.,

Sthenurus sp, nov., S. tindale’ (Wells & Tedford

in prep.}.

BIRDS: Dremaiidae; Dromiainus sp.

Dromarnithidae; Genyernis newtorir.

Unidentified smaller bird remains.

Tate (1893), Brown (1894), Stirling & Zietz

(1896, 1900). Stirling (1900, 1913), Howchin

(1930), Hale (1956), Tedford (1966, 1973),

Callen & Tedford (1976), Callen (1977), Rich

(1979), Wells & Tedford (in prep.)

17, BILLEROO CREEK 31°08’S,

(CURNAMONA}).

20 km SE of L. Frome. Red, sandy fluviatile Euri-

nilla Formation (Late Pleistacene). SAM, FUSA,

NMV, AMNHEL.

MARSUPTALS; Vurmbalidue; Lasiorhinus sp.

Thylacoleonidac; Tiyvlacaleo carnifex,

Diprotodontidae; Dipretadon sp.

Macropodidae; Betionyia sp., cf. Propleapus sp.-

Maeroapus sp.. M. cf. forragus, OspAranter sp.,

Sthenurus sp, noy,, 8. tindalet, Sthenuris sp., Pree

coptoden golial.

EUTHERIANS: Muridacy Lepurilluy sp.. Coni-

lurus sp.. Rattus sp. Pyeudomys sp,

BIRDS; Dromaiidue; Dramaius sp.

Dromornithidae; Genyornis newton.

Tate (1886), Callen & Tedford (1976), Callen

(1977), Wells & Tedford fin prep.)-

18. PERNATTY LAGOON 31°37'S,

(TORRENS).

SU km SE of Woomera. Weathered skeleton, Irag-

ments. SAM,

MARSUPIALS: Diprolodontidae; Diprotcdan sp.

Pledge (1974).

19. HOOKINA CREEK

(PARACHILNA)

25 km NW of Hawker. Valley-fill alluvium and

red pver-bank deposits of the Pooraka Formation

(Late Pleistocene). SAM, FUSA,

MARSUPIALS: Dasyuridae: cf. PDasycercuy sp.,

Surcomiilus sp. unidentified small dasyurid,

Peramelidae.

Vombuatidae; Lasiorhinus sp. ct. Wonibatuy sp.

Diprotodontidae; Dipratodan sp,

Macropodidae; cf. Petorays sp., Muacropus ef.

vigantens, M. cf eugenit, Macropus sp. Oy-

pheantwer sp.. Wallabia sp,, Propleopus oscillans,

unidentified small macropou,

40° 1S E

IST IGE

31%44'S, 138°14E

LOG Db, L. G. WILLIAMS

EUTHERIANS; Muridac; Aydromys chryso-

gaster, Leporillus conditor, Pseudamys hermanns-

burgensis, wildentified rodent.

BIRDS: Dromaiidae; Dromrainy sp,

Dromornithidac; Genyornis sp.

Unidentified small bird,

REPTILES: Elapidae; unidentified genus.

Varanidac; Varanis ef. glganteus,

Scincidaes Trachydosanrus sp. unideritified small

lizards.

AMPHIBIANS: Unidentified frogs,

FISH: Unidentified small fish,

Daily (1956), Twidale (1966), Williams & Polach

(1971), Williams (1973), Williams (in prep.).

20, MOUNT EYRE 31°46'S, 138°1'E (PARA-

CHILNA).

26 km NW of Hawker, Western piedinont slope of

ranges, Weathered skeleton on flat of sandy clay

SAM.

MARSUPIALS: Diprotodontidae; Dipretoder sp.

Daily (1954),

21. WILLOCHRA CREEK

(ORROROO).

8 km WS af Quorn, Encrusted skull, SAM.

MARSUPIALS; Macropodidae; Macropus sp.

22a, BOOLCUNDA CREEK 32°13'S, 138°18'E

(ORROROO).

“Lanewarren” 30 km NE of Quorn, Red clay and

gravel of dissected ovtwash fan. Mandible frag.

ment (casis). SAM.

MARSUPIALS: Diprotodontidac:

32°1S'S, 138°OS'E

LY gomalurius

sp.

‘Twidale (1966)-

22h BOOLCUNDA CREEK 32°/3'S, 138°3 °F

(ORROROO).

Unnamed tributary, 18 km south of Craddock.

VUSA,

MARSUPTALS; Macropodidae; Proceprodon sp,

Williams (in prep,).

2Zc HOOLCUNDA CREEK

138°30'S (ORROROO),

Note with specimen: “NE corner Mookra on Bool-

cunda Creek 50 ft below surface in sand with

Wish jn civernous part of munganite lode”

AUGM,

MARSUPTALS; Macropodidae: Pratemnaden sp-

23, BUICKALOWIE CAVES 32°08'S, 138°S5‘E

(ORROROU),

40 km SE of Hawker Maips Cave (B 3), Clara

St Deora Cave (F 4). Bone generally encrusted

with eulcite. SAM.

MARSUPIALS; Dasyuridae, Dasvurns sp., Sarce-

Pilla daeristé.

Thylacinidae; Thylacinus cynocephulas,

Peramelidae.

Thylacolennidae: Thylacolea carnifer.

Mactopodidue; Bellonwia sp,, Petarous sp., Macro-

pus sp.

upprox 32°20'S,

EUTHERIANS: Muridac,

BIRDS: Unidentified.

REPTILES: Unidentified,

Winton (1922),

24. TERTULPA 32°15'S,

MONA).

40 km NE of Yuntu. Note with specimen: “Brady's

Ciully Teetulpa, 14 feet from surface in the drift.

(888, SAM.

MARSUPIALS: Macropodidae; Proceptodon of

rapha,

Brown (1888).

25. DEMPSEY’S LAKE.

(PORT AUGUSTA),

§ km NW of Pt. Augusta. Red acolian sands of

the Pooraka Formation (Late Pleistocene), SAM,

PUSA,

MARSUPIALS: Dasyuridac} Dasyuris of, viver-

rinuy, Sarcophtilaus harrisii.

Vombatidae; Phascalonus cf. gigas, Lasiorhinus

latifrans.

Diprotodontidae; Pipretadoan sp.

Macropodidae; Beltongia lesueur, B. penicillate,

Macrapus sp.. Macropas cf. ferragus, Osphranier

sp., Protemnodon brehus.

BIRDS; Dromajiidac; Praniaius sp.

Dromornithidue; Genvornix sp.

7Anatidac,

REPTILES: Elapidae,

Scincidae;: Trachydosaurus sp.

Cooper (1959), Williams

(1976).

26. ARNOLD'S BANK 32°22'S, 137°46'E (PORT

AUGUSTA),

15 km north of Pt, Augusta, Red sand dine in

area of dunes and salt flats, head of Spencer Gulf.

Pooraka Formation (Late Pleistocene), SAM.

MARSUPIALS: Diprotodontidae: Dipratedan sp-

Williams (1976).

27. YJAILLPARA CREEK

{ORROROO),

30 km NE of Orrarda. Red clayey alluvium asso-

clated wilh creck. SAM,

MARSUPIALS: Diprotodontidae; Piproledon sp,

Macropodidae; Sthenarus sp.

Hale (1956), Daily (1960b), ‘Iwidale (1966),

Williams (in prep,).

28. NECTAR BROOK 32°42’S, (37°56 (PORT

AUGUSTA).

78 km SSE of PL Augusta. Red ulluvium exposed

during dam excavation in 1898, SAM,

MARSUPIALS: Diprotodontidae, Miprotoden sp.

Macropodidve; Maecropus sp.

29, PEKINA CREEK 32°44'S, ]38°37E

fORROROO)

2 km south of Orroroo, Greenish lacustrine clays

exposed on SE shore of reservoir, and poorly-

sorted alluvium below dam wall. Macropus sp. his

139°41"E (CURNA

137°42°B

32°28'S,

(1973), Williams

32°S1'S, |38°S5'E

PLEISTOCENE VERTEBRATE FOSSILS 107

also been recovered from 4 well excavation 18 m

deep on Pekina Creck floodplain. SAM, FUSA,

MARSUPIALS: Vormbatidae,

Diprotodontidae; Dipreteden sp.

Macropodidae; Bellanxia sp.. Macropus sp.

Howehin (1909), Williams (in prep.)

30. BLACK ROCK GRAVEL PIT 32°47'S, 138°

40'E (ORROROO),

8 km south of Orroroo, Distised! gravel pit on allu-

vial plain, Sinuous channel deposit of fine, rouniled

gravel with red sundy matrix. SAM,

MARSUPIALS: Diprotodontidae; Diprotedan sp

Macropodidac; Mucropus sp., Prolemnaden ‘ps

Sthenurus sp.

31, MANUNDA CREEK 32°56'S.

(ORROROO),

40 ko cast of Peterborough, Red clayey overbank

deposit af creek. SAM,

MARSUPIALS: Macropodidae; Proeoptaden sp.

Edwards (1964),

32, PORT PIRIE GRAVEL PIT 32°15'S, 133°

05'B (BURRA).

3 km south of Pt, Pirie, Western flank Of ranges.

Clean coarse quarts gravel, SAM.

MARSUPIALS: Thylacoleonitue: Vhwlacolea sp.

Diprotodontidae, Diprotedar sp-

Macropodidac; = Macopuy sp, M. cf,

Sthenurus sp.

Pledge (1973, 1974).

33. WAUPUNYAH CREEK 93°15, [39°05 'E

(BURRA).

8 km cast of Terowie. Red clayey alluvium of

creck. SAM, TUSA,

MARSUPIALS: Vombatidae: cf, Lastoriinns 5p,

Diprotodontidae: Diprotodon sp,

Macropodidac; Macrapus spp, Osphranter sp.

Pracaptodon sp.

Williams (in prep.).

34, ULOOLOO 33°19'S, 138°53'E (BURRA),

35 km north of Burra, Piedmont and alluvial

depasits of Irwin and Terowie Creeks. SAM,

FUSA.

MARSUPIALS: Diprotodontidae; Diprotadon sp,

Macropodidaes Pracepladon sp.

Williams (in prep.).

35. COLLINSVIELE 33°20'S, [39° 08'E

(BURRA),

50) kin NE of Burra. Red silty floodplain deposit

in Witt Creek valley, expoyed by modern gully-

ing. SAM, FUSA,

MARSUPIALS: Diprotodontidae, Miproradon sp.

Micropodidue; Macropus spp. Procapladen sp.

Williams (in prep.).

46, NEWIKIE CREEK 33°30'S, 139° 10°E

IBURRA)

25 km NE of Burrs, Alluvial fan sands ond

provels. SAM, PUSA.

MARSUPIALS: Vombalidue; Lasiariinis sp-

139°21E

furan,

Diprotodontidue; DBipretocden sp

Macropodidae,

Williams (in prep.)-

37, BALDINA CREEK 33°41'S, 139°U4'E

(RURBRA),

13 km east of Burra, Red silty valley alluvium. anu

fan, SAM, FUSA.

MARSUPIALS: Vombatidaes Lasiorhinis sp,

Thylucoleonidae; Thylacolea carnifex,

Diprotodontidae; Dipreraden sp.

Mactopodidae; Beftongia sp., Macropus sppo Pro-

remnodon sp, Sthenurus cf. atlas,

BLRDS: Dromornithidae; Genyornis newlenit

Vare (1890), Zietz (1890), Stirling & Ziete (1896,

1913) Stirling (1900), Howchin (1930), Hale

(1956), Rich (1979), Williams (in prep.),

38. BUTE 33°52’S, 138°01'R (BURRA).

20 km SW of Snowtown, Material associated With

human remains A25805, from a sand dune, Prob-

ably Holocene, Anthropology Collection. SAM.

MARSUPTALS: Macropodidae; Macrayiis sp,

BIRDS: Dromuaiidae; Yramalus sp,

49. BURRA CREEK 33°52'S, 139°09 E

(BURRA),

30 km SE of Burra, Brown silts, sands, and gravels

of alluvial fan. FUSA,

MARSUPIALS: Diprotodontidae; Diprotedon sp.

Macropodidite.

REPTILES: Unidentified small lizards.

AMPHIBIANS: Unidentified frogs,

Chapman & Mawson (1925), Williams (in prep.),

4), BUNDEY 33°53'S, 139° L8E (BURRA),

40 Km SE of Burra, “Gum Creek”. Red clay ex-

posed by dam excavations in L889 and 1953,

SAM.

MARSUPIALS:

UTNTHUS,

Thylacoleonidae: Thylacalea carnifer,

Diprotodontidae: Diproteden spp(?),

Mucropodidae; ?Sthemurus sp-

Zicté (1890), Stirling £1900), Howchin (1930).

Pledge (1977), Williams (in prep.).

41, MORGAN 34°02'S. 139°40°E (RENMARK)

River Murray flats, north bank, where eliffs are

cut by tribatary fram the NW. SAM.

MARSUPIALS; Vombatidue; Phascolanuy sp.

Diprotadontidae, Bipretodon sp.

Mactopodidse; Macropus sp.

N.S, Pledge (pers. comm, 1979).

Dasyuridae; Surcephilus ef,

42, CHOWILLA 34°01'S, 140°50°R (REN-

MARE),

North of Renmark. Excavation for proposed

Chowilla Dam wall, [8 m deep. SADME

MARSUPIALS;: Vombntidae: Phascolonus sp.

Firtnun (1966), Marshall (1973).

43. CURRAMULKA 34°42'S, [37°44'E (MAITT-

LAND),

a. Town Cave (¥ 2) jn Curramutka. Red, stony

18 D. L, G, WILLIAMS

clay With flowstone. Bone generally enerusted with

calcite. SAM, FUSA, LICMP,

MARSUPIALS: Duasyuridaes Desvurns sp.

Peramelidae; Perameles sp.

Vombatidac: Lasiorhinns sp,

Thylucoleonidac; Tivlacolee carnifex, V. hilli.

Diprotodontidae: cl. Notarherlum sp,

Macropodidae; Mucropus sp., Prateninadon syn,

Wallabia sp.. Sihenurus spp.. Procaptoden sp,

EUTHERIANS: Muridae.

b, Quarry 2 km south of Curramulka, Red cal-

cite-cemented bone breccia filling fissures in Early

Cambrian limestone. SAM, FUSA,

MARSUPLALS: Vombatuae; Lasiverhinus sp.

Macropodidae; Macrapus sp., Procopledon sp,

Pritchard (1491). Howchin (1925), Dally (196Da.

W60b}, Pledge (1977),

44. LARE FOWLER 35°15°S, 137°37'E (KINGS.

COTE),

Southern Yorke Peninsula, Gypsum lunette on east

shore of lake, Fossils exposed by quarrying. SAML

(J, A. MeNamara (974. Undergraduate project,

Zoology Dept, University of Adelaide, unpub,)

MARSUPIALS: Dasyuridve: Sareophilus ef

ursitus,

Peramelidae; Macrotis cf, lavelis,

Vombatidac; Lasorltiinus sp.

Thylacdleonidae; Thylacelee earnifer,

Macropadidac, Belionuia lesueur, Macropuy et.

ferrayus, M. cf evgenli, Onychogalea sp.

EUTHEFRIANS: Muridac; Leparillyus sp.

Howchin (1900), Jack (1921), King (1950),

45, PONDALOWIE BAY 35°14'S, 136°50'F

(KINGSCOTE).,

SW Yorke Peninsula, near one of the Jakes at

Pondalowie, Calearedus chiystone slab with track-

ways. ?Holoceno.. SAM,

MARSUPIALS: Macropodidac: ?Maerapus sp.

BIRDS: Dromaiidaes ?Bromatus sp

46. ROCKY RIVER 35°55'8, 136°47°E (KINGS-

COTE),

Western end of Kangaroo Island. Swamp deposit.

SAM,

MARSUPIALS: Dasyuridae; Sareaplilus sp.

Vombatidae; Unidentified genera,

Phascolarctidaes Phaseolaretos cinereus,

Phalangeridae; Trichosurus valpecule,

Diprotodontidae; Diproieden sp..

trilohius,

Mucropodidae; Macropus fuliginosus, M- engenti,

Pratemnodon sp, Sthenuray spp. S. gilli.

EUTHERLANS: Muridae,

BIRDS: Dromaiidae; Premaluy sp-

Jones (1923) Tindale ef al. (1995), Hale (1956)-

Pledge (1975, 1979), J. BR. Hope (pers. comm.

1980),

47, KELLY HILL CAVES (K 1-4, 14d, 44)

35°S9S, 136°54’E (KINGSOCOTE).

SW Kangaroo Island. SAM,

Zygamatary

MARSUPIALS: Dasyuridac. Dasyurus maculatas,

Sarcaphilus harrisii, Phascogale tapoatafa.

Vombatidue; Lasiorhinus sp,

Phascolarctidacs Phascolarctos cimercus.

Phalangendae; Trichosuras vulpecula.

Petauridae; Pseudocheirns peregrinus,

Macrapodidae; Murrapys fulizinosus, M. eugenil,

Srhenurus ch. ovcidentalis,

BIRDS; Dromaiidac; Uromaius diemenianus.

Howehin (1930), Hale (1956), Hope er al.

(1977), Pledge (1979), R. T. Wells (pers, comny.

1974),

48a. MOUNT TAYLOR CAVE (K&) 35°58'S,

(37°03 E (KINGSCOTE).

SW Kangaroo Island, 5 km east of Mt Stockdale.

SAM,

MARSUPBIALS: Macropodidae: Sihenurns sp.

Pledge (1979),

48b. EMU FOUR HOLE CAVE (K 20) 35°59'S,

136°54'E (KINGSCOTE),

SW Kangaroo tsland, near Mt Taylor, Subfogsil ta

modern hones (Pledge 1979), SAM.

MARSUPLALS: Dasyuridae; Dayvurus viverrinis,

Sminthapsis murina,

Peramelids; Perameles sp.. fsoodon obesutus.

Phalangeridae; Trichosurus vulpecula.

Petauridac; Pyeudocheiruy peregrinus,

Burramyidae; Cercartetus concinnus.

Macropodidae, Poterous platyaps, Macropuy fuli-

rinasus, M. eugenit.

MONOTREMES: Tachyglossidac;

aculeatus,

RUTHERIANS; Muridaez Ranus fuscipes, R,

lutreolus.

BIRDS: Dromnaiidae; Bramualis diemenianus,

Hale (1956), Pledge (1979)

48¢. FOSSIL CAVE (K21t) 35°59'S, 136°S4’E

(KINGSCOTE).

Adjacent to Emu Four Hole Cave. SW Kangaroo

Island, SAM,

MARSUPIALS; Dasyuridae; Sarcophilus cf har

resin.

Vombatidae,

Phascolarctidae; Phascelarctos cinereus

Macropodidac: Maecrapus fuliginosyus, M-. eugenil,

Sthennrus cf. hrowrnel.

EUTHERIANS: Muridae,

Pledge (1979),

48d, SETON ROCK SHELTER (K 30) 35°59'S,

137°03'E (KINGSCOTE),

SW Kanguroo Island, Archaeological; sandy sedi-

ments excavated to a depth of about 27 m. SAM.

MARSUPIALS: Dasyuridace: Oasyuruy — cf,

geaffroi/vivereiins, Bo maculatus, Sarcaphilus har-

risil,

Peramelidae, Perameles borgainviile, tscodon ube

sulas,

Vombatidue;: Lasfarhimey latifrans

Phalangeritae: Trichosueus vulpeewta,

Burramyidae; Cerearterus lepidus,

Tachyglossus

PLEISTOCENE VERTEBRATE FOSSILS 19

Macropadidae; Bevongla penicillata, B. lesueur,

Potorous platveps, Macropas ct. Jaliginosus, M-

greyi. M. rujagrisens, cf. Mepaleia rufa, Lagor-

cheses leporides, Sthenurus cf, gilli,

FUTHERIANS, Mouridae, Afydranys ¢liryse-

waster, Raras pusoipes ereyi, Ry hettecdlas, Mastar

comus fuscus, Pseudoms occidentalis, PB. austra-

lis shortridget.

BIRDS: Procellanidae; Pachyptila cl. salvint, Puf-

finis sp,

Platalwidues Tireskiornis cf, molneca.

Anulidae, ef 4aseranas semipalmaia, Vaderna cf,

nidornoides, Anas v& superciliosa, Anas et, cs-

tanea. Malacarhynelins menbranacers.

Accipitridae; Mieradetus morphinoides.

Falconidae; Falce berivare.

Phasianidaes Coturule cf, pectoralis.

Turnicidacy Turnix varia, T, velox

Rallidae; Ratlus philippensis, R. pectoralis, Par-

sauna ef, fuminea, Gallinula (Tribanyad cf. mor-

lierti, GO, (Tribonyx) ef. ventralis,

Burhinidues Burhinusy mrageinasiris,

Scolopacidae; Gullinugo cf, harilwiekt.

Laridae; Larus noviehollandive, Sterna cf, nereis,

Columbidac: Ocyphups lophates.

Platycercidas; Pezoporus wallicus, Cathamus dis-

colar.

Hirtindinidae; Mirunda cf. taliticn, Petrechelidon

nigricans.

Meliphagicae,

Sylviidae; Cinclerhamphus eruralis.

Grallinidae: Grallina evanalenca,

Cracticidue,; Gyniiorliina dibicur, Slrepent gracu-

lina, 8. versicolor.

Corvidae; Corvus sp.

Unidentified passerines.

REPTILES: Elupidae.

Varanidac: Maranis sp.

Scincidue; Trachydosauras rugexus. Tiliqna niveo-

lutea, cf Egernia whitii.

Agamidaes 4mplibolarus spp.

MOLLUSCS: Marine molluscs of archacologicil

origin, and terrestrial/aquatic molluscs

Hope eral. (1977),

49, HOG BAY RIVER

(KINGSCOTE).

Eastern Kangaroo Island, Found in “Pleistocene

drift’ (Cutulovuc!, SAM.

MARSUPIALS: Mucropodidae, Macrapus sp.

as°49'S, 197"57’E

50, KAPUNDA 34°23'S, 139°00E

(ADELAIDE).

South of Kupnnda. Bones and teeth in matrix.

SAM.

MARSLIPIALS: Vombatidue; Phascolonas sp-

Jack (191%), lohns (1947).

5). TWO WELLES 34°36°S,

LAIDE),

35 km north of Adelaide. Sandpit “near Two

Wells” (notewith mandible), SAM,

MARSUPIALS: Diprotedontidae; Diprvfodent sp.

138°3'ER (ADE-

52, GAWLER 34°35'S, 138°45'E (ADELAIDE)

40 km north of Adelaide. Excavations on banks of

Gawler and South Para Rivers. SAM.

MARSUPIALS: Diprotodontidac: Diprotodon sp.

Stirling (1900). Howehin (1930), Hale (1956)-~

53. YATALA 34°51'S, 138°37E (ADELAIDE).

NE suburb of Adelaide. Jaw “9 feet below the

surfuce in 4 bed of gravel” (Moncrieff 1882). Lo-

cation of specimen unknown.

MARSUPIALS: Diprotodontidae; Diprotoden sp.

Moncrieff (1882),

$4. FROMM’S LANDING 34°46'S,

(RENMARK).

River Murray, near Walker Flat. Archaeplogical;

rock shelter. SAM,

NOTE; The assemblages summarised here do nor

distinguish the numerous straugraphic levels

recognised by Mulvaney er al. (1964).

i, Shelter 2.

MARSUPIALS: Dasyuridae; Duasyurus peoffrai,

Dasyuropy maculatus, Sarcaphilus harrisii,, Dasy-

cercus eristicaudata, Antechinus flavipes, Av swain-

soni, Sminthopsis cf. murina, Myrmecobius fas-

cians.

Thylacinidae; Thylacinus eynacephalis.

Peramelidac; Peramelex bougainville. cf

obesulus, Chueropus ceaudatus,

Vormbatidue; cf. Lasiorhinus latifrons.

Phalangeridae; Trichosurus vulpecula-

Petausidac; Pseudocheirus peregrinuy.

Macropadidac; Retlongiy penicillaia, B. lesueur,

Pororous margani, Macrapus canguru, Thylagale

engenii, Onychogalea lunata, Lagorehestes lepo-

ridvs, Lagastrophus [aseiatus.

EUTHERIANS: Canidae; Canis fanniliaris dingo.

Mutidae; Aydromys chrysogaster, R. greyl, Rattus

luireolus, cf, Psendomys auritus, Thetamyy gp. cf.

Noatemys sp., Contlurus albipes.

Mulvaney er al. (1964), Archer (1971).

b. Shelter 6.

MARSUPTALS: Dasyuridae:

elaius,

Peramelidae; Perameles hougainville, Iyaodon obe-

srlus, Chaeropus ecaucdatiiy.

Phalangeridae; Trieliosurus vulpecula,

Macropodidae; Relrongia penicillata,, Macrepus

canguru, Thylogale ecugenti, Lagorchestes lepo-

rides, Lagostrophus fasciatus,

EPUTHERIANS: Canidae; Caniy familiarts dingo.

Muridae: Hydromys chrysogaster, R. grey’, Rattus

fatrealus:

Mulvaney ef al, (1964),

139°33'E

lsoodon

Myrmecebius as-

55, DEVON DOWNS 34°41'S, 139°37'E (REN-

MARK).

River Murray, nocth of Mannum. Archaeological;

rock sheller, SAM. Note: The assemblages suam-

marised here do not distinguish the numerous

stratigraphic levels recognised by Hale & Tindale

(1930), See also M. Smith, 1977 B.Sc. (Hons)

1d BD. L. G. WILIJAMS

thesis, Avst. Nat. Univ, Dept of Prehistory &

Anthropology (impub,),

MARSUPIALS: Dasyuridae; Dayyvurw viverrinicy,

D. geoffroyi, Sarcophilus harrisii, Phaseagale flax

wipes,

Peramelidae;

sulus,

Vombutidae;, Lasiorhinus sp.

Phalangeridae; Trichosaris Vulpecila,

Petauridae; Psevdocheirus sp-

Macropodidae, FRettongia sp, Poterons $f.

Muacropus sp, Mucropus cf. sigantens, Thylexule

sp.. Lagerchestes leparides,

EUTHERIANS: Canidae; Canis familoriv dinge.

Muridae; Hydromys elhuysegester, Rattus sp.

BIRDS: Dromaiidae; Dromains novuehallanediae-

Anatidae; Querquedula sp.. Chenopis alrwta, Br-

giuvra lobata.

Accipitridae; Urogeruy anedice-

REPTILES: Boidae; Python spilars.

Vuranidae; Varanty cf, eouldii.

Scincidae: Trachysaurus rugosa, Tiliqna sp,

Agamidae; Ampliholurus sp,

TORTOISES: Chelidue; Chelodina

Emydura maequarti,

FISH) Maceullochellidue; Oliguins macquariensis.

Plotosidae: Tyndarus nonelents.

Plectroplitidaes Pleerroplite, ambleuns.

INVERTEBRATES: A range of molluscs ane

crustaceans.

Hale & Tindale (1930).

56, CHUCKA BEND 34°53'S, 139°39'E (REN-

MARK),

River Murray, north of Mannum. Site details and

location of specimens unknown,

MARSUPIALS: Vombatidae; Pliascolonuy sp-

Stirling (1913), Howehin (1930),

57, ADELAIDE AREA 34°55’S, 138°35°E (ANP-

LAIDE)..

A number of sites which appear to be associated

with alluvium of the River Torrens.

a. Allenby Gardens 34°53’S, 138°34°E (ADE-

LAIDE),

Adjacent to NW corner of Adelaide city. Speci-

mens found “Approx. 20 ft, below the surface”

(SAM Catalogue).

MARSUPIALS: Diprotodontidae; Dipraradon sp.,

ef. Nototherivim sp,

bh. Brompton 34°54'S, 138°34°R (ADELAIDE),

Adjaceat to NW corner of Adelalde city: 20, East

Street, Brompton, Note with specimens, "25 feel

below surface" In black clay, SAM,

MARSUPIALS; Diprotodontidae: Diprorodon sp

c. Croydon 54°53°S, |38°34E (ADELAIDE),

Adjacent to NW comer of Adelaide city. Several

localities “within two and three miles of Croydon"

(Tate 1890), "Found on Mr Woodhouse’s pro-

perty (South of Railway line West from Croydon

Railway Station) at Croydon about 4-6 fe helow

the surfuce in an old river bed Of shurp sane and

sravel™. (Note with specimens.) SAM,

Perameles myoyara, Isaode Abie

longicallis,

MARSUPIALS: Vombutidaes cf, Phascolomyy sp-

Diprotodontiduey Diprereadon sp.

Tate (1890),

d. Findon 34°55°S, 138°32'R (ADELAIDE).

Western suburb of Adelaide, One of numerous

gravel pits, SAM,

A Vombatidae; Unidentified man-

(ile,

Dipretadontidae; Diprolodar sp,

HERDS: “Bird bone” catalogued,

Howchin (1913),

c. Kirkaldy Pit

LAIDE).

Western suburb of Adelaide, One of numerous

gravel pits. SAM.

MAKSUPILALS: Diprotodontidae; Diprotadon sp,

{ Thebarton 34°55'S, 138°34'E (ADELAIDE)~

Adjucent 1 west side of Adelaide cily, Rib bone

from “a depth of six feet” (Waterhouse (882)

Origin of P, azael jaw not known. SAM.

MARSUPIALS: Diprotodontidae; Pularehestes

vzuel.

Waterhouse (1882)-

58. HALLETT COVE 35°04'S, 138°30'E (ADE-

LAIDE).

Southern coastal suburb of Adelaide, Waterworn

molar from modern heach gravel, derived from

cliff exposures of Pleistocene sediments, SAM,

MARSUPIALS: Diprotodonmtidae: Diprotodon sp-

54, ECHUNGA 35°06'S, 138°48'E (BARKER).

30 km SE of Adelaide. Bone from "deep plluvium"

{note with specimens), May be Tertiary. SAM.

MARSUPIALS: ?Mucropodidae.

60a. SALT CREEK 35°28'S, 138°20°R

(BARKER)

80 km south of Adelaide, Sulphurous black clays

of swamp deposit. There is a New Salt Creck

“four miles north of Cape Jervis” (Hale 1946),

but Brown (1892) leaves no doubt that the site

is near Normanville. SAM,

MARSUPIALS: Vombatidae; Phaseolonus givas.

Thylacolvonidae: Thvlacalee carnifex,

Diprotodontidae; Diprefedan sp.

Macropodidae, Berfongia sp., Macrepus sp, Os-

plranter sp., Sthenurts sp., Procaptodon sp,

BIRDS: Drompiidae; Drameains sp.

Dromorhithidae: Geayorniy newton,

Unidentified bird remains.

REPTILES: Unidentified material.

FISH: Unjdentified material,

Waterhouse (1880), Brown (842), Stirline &

Zietz (1896). Zictz (1907), Stirling (1913), How-

chin (1930), Hale 11956), Ride (1967), Pledee

(1977)

hb, YANKALILILA 35°28'S, 138°37°E

(HARKER.

KO kin south of Adelaide. Possibly rhe same site as

Salf Creek. SAM.

MARSUPIALS: Diprotodontidae: Plprotedan sp,

34°55'S, 38°30°R (ADE.

PLEISTOCENE VERTEBRATE FOSSILS I

61. GOOLWA 35°31'S, 138°45°E (BARKER).

70 km south of Adelaide. Known as the “Goolwa

Footprints”, specimens actually taken from an

eroding cliff at nearby Middleton Beach in 1938,

Exposed below ubout 7 m of “sands, limestones

ete. above the pipeclay on which the prints were

made,” (Letter by Fenner, 20th June, 1952; copy

wilh originals and casts.) SAM,

MARSUPIALS: Unidentified footprints, approx,

150 mm long.

62. BLACKFORD DRAIN 36°46'5,

(NARACOORTE).

21 km NE of Kingston, $.£. During placement of

bridge pylons, fossils recovered from }i depth of

“11-13 feet", north side of creek, in a bed of

waterworn stones. “Rock bottom” at 13 feet Was

“a hard stone which looked like u flow of black

mud, thickly impregnated with small white shells”.

(Letter from R, V. Flint with specimens.) SAM,

MARSUPIALS: Diprotodontitae: D/preradon sp,

Macropodidue; Macropus spp., Stltenurvs sp. ct,

Procoptodon sp.

1d0°OE

63, NARACOORTE, 36°59'S, [90°45 F 1 NARA-

COORTE),

SE South Australia, Cave Sites, SAM.

a, Henschke’s Bone Dig (U 91/97) Gutskirts af

Naracoorte at Hensehke's Quarry A diverse

assemblage, mostly marsupial. Differs in detail

from Naracoorte Caves deposits. (N. S, Pledge

ners, comm, 1979), SAM.

MONOTREMES: Tachyglossidae; Zaglassus rumt-

Saye,

BIRDS: Megapodiidae, Progura naracoortensis.

AMPHIBIANS: Hylidae; Litaria ewinsi,

Leptoductytidae; Limnadynastes — fasmantlensts,

Ranidella signiferd.

van Tets (19740), Tyler (1977), Pledge (in prep.),

b. James’ Quarry Cave [U 29), Naracoorte

township, UCMP.

MARSUPIALS: Thylacoleonidue: Thylacalee car-

nifex.

Daily (1960a)

fd. NARACOORTE CAVES 37°(1'S,

(PENOLA).

(5 km SE of Naracoorte, Numerous caves, ususlly

with red sundy cave fill containing fossils. SAM,

FUSA,

a, Alexandra Cave (1/3).

Old collections SAM. Recently collected: FUSA-

MARSUPIALS: Thylucoleonidae: Tlrylacolew rur-

nifece.

Macropodidue; Sthenurus cf. oceldentalis, Sthenn-

rus sp., Pracoptodon sp.

b. Brown Snake Cave (U 14),

SAM collection.

MARSUPEALS: Macropadidae, Vrienuries sp,

c. Cathedral Cave (U 12/13),

SAM callection,

14 48'F

MARSUPIALS: Thylacoleanidae, Thylucolea ear.

Nifex.

d, Dogs Prohibited Cave (U —-).

FUSA collection.

MARSUPIALS: Dasyuridac, Dasyirids sf,

Perumelidue.

Macropodidae; Porarons sp, Mucropiy sp,

EUTHERIANS: Muridac,

BIRDS: Unidentified material,

é. Fox Cave (U 22).

SAM collection.

MARSUPIALS: Dasyuridae: Desyverus sp. Sarees

phils sp.

Thylacinidue: Thylacinuy sp.

Peramelidac; Isacean sp,

Vombuatlidac: Varnbaius sp,

Phalangeridae; Trichosurus sp.

Petauridae, Prendocheirus sp.

Thylacoleonidae; Thylacalea earnifex,

Macropodidiue; Beitonyia sp., Pelorous sp, Macre-

pus cf, givantéus, M_ rufegrisens, Sthenueus sp., 8.

willl,

BIRDS; Unidentified material,

f. Haystall Cave (U 23).

SAM collection.

MARSUPIALS: Dasyuridae: Dasvurus sp. Saree-

plulas lantaritas,

Phascolarclidue; Phascolarctas sp,

Thylacoleonidaes Thivlacaled sp.

Macropodidaec: Macropus sp.. Stleaurus sp.

REPTILES: Scincidae; Viliqua sp.

g. Specimen Cave (U 35).

Previously known as Zietz Cave, SAM.

MARSUPIALS: Dasyuridue: Sareophiluy lari-

aris,

Thylacinidae; Thvlactiusy ct, major.

Peramelidae.

Vombatidae.

Thylacoleanidae: Tlvlacelee sp.

Mucropodidac; Macropus sp,, M. ef,

temiriodon ef, anak,

h. Tomato-Stick Cave (U 10/11).

SAM collection.

MARSUPTALS:

Protemnodon sp,

(ilan, Pros

Macropodidae: Marropus sp,

\, Victoria Fossil Cave (U 1).

SAM, FUSA collections,

MARSUPIALS: Dasyuridae: Dasyurns viverrinuy,

PD, maculatus, Sarcophilus sp., Antechinus Havipes,

A. stuartii., A. swainsonii, Sminthopsis crassi-

candata, S. murina.

Thylacinidaes Thylueinus evnocephaluy,

Peramelidue: Perameles sunnii, PP) bodeainville,

Isoodon abesulis.

Vombatidie; Vonthatits sp,

Phascolarctidac; Phaseolaretas sp.

Petauridae; Psendocheirns pereerintus,

hreviceps.

Burramyidae; Ceroarntus nanus,

Thylacoleonidae: Th ylacolee carnifex

Peanuts

112 D. L. G. WILLIAMS

Diprotodontidae; Palorchestes azael, Zygomaturus

trilobus.

Macropodidae; Bettongia penicillata, B. gaimardi,

Potorous apicalis, P. platyops, Macropus gigan-

teus, M. rufogriseus, M. greyi, M. eugenii, M.

titan, Wallabia bicolor, Protemnodon roechus,

Sthenurus andersoni, S. atlas, S. brownei, S. gilli,

S. maddocki, S. occidentalis, Procoptodon rapha,

small macropods.

MONOTREMES:

sp., Zaglossus sp.

EUTHERIANS: At least six species of rodent

(M. J. Smith in prep.).

BIRDS: Dromaiidae; Dromaius novaehollandiae.

Megapodidae; Progura naracoortensis, Leipoa

ocellata, indeterminate species.

Phasianidae; Coturnix pectoralis, C. australis.

Turnicidae; Turnix sp., T. varia.

Pedionomidae; Pedionomus torquatus.

Rallidae; Rallus philippensis.

Charadriidae; Peltohyas australis.

Scolopacidae; Tringa_ glareola,

wickii, Calidris ruficollis.

Platycercidae; Pezoporus wallicus.

Tytonidae; Tyto novaehollandiae.

Grallinidae; Grallina cyanoleuca.

Craticidae; Gymnorhina tibicen.

REPTILES: Boidae; Wonambi naracoortensis.

Elapidae; Pseudonaja cf. nuchalis, Notechis cf.

scutatus, Pseudechis cf. porphyriacus, Unidentified

group,

Varanidae; Varanus varius, V. gouldii.

Scincidae; Trachydosaurus rugosus, Tiliqua nigro-

lutea, cf. Sphenomorphus tympanum, Egernia cf.

whitei.

Agamidae; Amphibolurus cf, barbatus.

AMPHIBIANS: Hylidae; Litoria ewingi.

Leptodactylidae; Limnodynastes cf.

Ranidella signifera, Geocrinea cf. laevis.

Woods (1866), Smith (1971, 1972, 1976), van

Tets (1974a), van Tets & Smith (1974), Wells

(1975), Olson (1976), Wells & Nichol (1977),

Tyler (1977), Murray (1979), Wells & Murray

(1979), Wells (pers. comm, 1979),

65. PENOLA 37°23’S, 140°50°'E (PENOLA).

22 km NNW of Penola. Bones found in sinking a

well on the edge of a swamp. Whereabouts of

fossils unknown.

BIRDS: Dromornithidae; cf. Genyornis sp.

Stirling & Zietz (1896, 1900), Rich (1979).

66a. GLENCOE 37°41’S, 140°37'E (PENOLA).

22 km NW of Mt Gambier. Probably a cave depo-

sit, as fossils are white with red sediment adhering.

Possibly Glencoe West Cave (L77) or Glencoe

East Cave (L108). SAM.

MARSUPIALS: Macropodidae;

Sthenurus sp.

Tindale (1933).

66b. GREEN WATERHOLE

140°32’E (PENOLA).

22 km NW of Mt Gambier. Also known as Fossil

Tachyglossidae; Tachyglossus

Gallinago hard-

dumerili,

Macropus sp.,

(L 81) 37°44’S,

Cave. Fossils from surface of rockpile to a depth

of 15 m in water-filled cave. SAM, FUSA.

MARSUPIALS: Dasyuridae; Dasyurus sp., Sarco-

philus sp.

Thylacinidae; Thylacinus sp.

Phalangeridae; Trichosurus sp.

Thylacoleonidae; Thylacoleo carnifex.

Macropodidae; Bettongia penicillata, Propleopus

oscillans, Macropus sp., Osphranter sp., Protem-

nodon sp., Wallabia sp., Sthenurus gilli, S. mad-

docki, S. occidentalis,

EUTHERIANS: Muridae.

BATS: Unidentified material.

BIRDS: Dromornithidae; ?Genyornis sp.

A diverse assemblage of other birds.

Wells & Murray (1979), Wells & Williams (in

prep.), Rich & van Tets (in prep.), Pledge (in

prep.).

66c. MILLICENT 37°36’S, 140°21’E (PENOLA),

Far SE of South Australia. Fossils found “at a

depth of six feet below the surface, embedded in

peat mixed with shells” (Waterhouse 1882).

Accession card for SI states “18 in. below sur-

face”.

MARSUPIALS: Diprotodontidae; Diprotodon sp.,

Zygomaturus sp.

Waterhouse (1882).

66d. MT BURR CAVE (L 69/70) 37°32’S, 140°

27'E (PENOLA).

Far SE of South Australia. SAM.

MARSUPIALS: Macropodidae; Sthenurus sp.

66e. TANTANOOLA CAVE (L12) 37°43’S,

140°30’E (PENOLA).

Near Tantanoola. Cave

SAM.

MARSUPIALS: Dasyuridae; ?Sarcophilus sp.

Vombatidae; ?Phascolomys sp.

Phalangeridae; Trichosurus sp.

Macropodidae; Sthenurus — sp.,

roechus.

EUTHERIANS: Otariidae; Arctocephalus sp.

Muridae; Rattus sp., Hydromys sp.

Tindale (1933).

in old wave-cut cliff.

Protemnodon

67. MOUNT GAMBIER 37°50’S, 140°47'E

(PENOLA).

Far SE of South Australia,

a. Cave exposed by earthworks in Derrington

Street. SAM.

MARSUPIALS: Peramelidae; Perameles sp.

Phascolarctidae; Phascolarctos sp.

Phalangeridae; Pseudocheirus sp.

Thylacoleonidae; Thylacoleo carnifex.

Diprotodontidae; Nototherium sp.

Macropodidae; Bettongia sp., Sthenurus spp.

b. Cave, location unknown. BMNH.

BIRDS: Dromornithidae; Genyornis sp.

Stirling & Zietz (1896, 1900), Rich (1979),

PLEISTOCENE VERTEBRATE FOSSILS 113

c. Cave exposed by excavation in Gray Street.

SAM.

MARSUPIALS: Sthenurus spp.

d. Moorak 37°52’S, 140°47’E (PENOLA),

5 km south of Mt Gambier. Probably a cave

deposit. SAM,

MARSUPIALS: Thylacoleonidae; Thylacoleo sp.

Macropodidae; Sthenurus sp.

Adelaide area 53, 57, 58.

Alexandra Cave 64a.

Allenby Gardens 57a.

Arnold’s Bank 26.

Baldina Creek 37.

Billeroo Creek 17.

Blackford Drain 62.

Black Rock Gravel Pit 30,

Boolcunda Creek 22.

Brompton 57b.

Brothers Islands 3.

Brown Snake Cave 64b.

Buckalowie Caves 23.

Bundey 40,

Burra Creek 39.

Bute 38.

Calca 2.

Cannatalkaninna | la.

Cassidy Locality 7a.

Cathedral Cave 64c.

Channel Sand Locality 12a.

Chowilla 42.

Chucka Bend 56.

Clara St. Dora Cave 23.

Collinsville 35.

Cooper Creek 11.

Cootanoorina 9.

Croydon 57c.

Curramulka Cave 43a.

Curramulka Quarry 43b.

Cuttapirra Waterhole 11i.

Dempsey’s Lake 25.

Devon Downs 55.

Diamantina River 5, 6.

Dogs Prohibited Cave 64d.

Echunga 59.

Emu Four Hole Cave 48b.

Findon 57d.

Fossil Cave 48c,

Fox Cave 64e.

Fromm’s Landing 54.

Acknowledgements

The author is indebted to Dr R. H. Tedford

for additional data on the L. Eyre region, and

to Ms K. Mackenzie for typing the MS.

68. 72TANKSTAND CAVE (L 65) 37°57’S, 140°

40’E (PENOLA).

3 km west of Mt Shank; ‘Sec 823, Hd Macdon-

nell, Co Sturt” (SAM Catalogue). However, this

should probably be County Grey, where there are

numerous caves (Hundred Map, H. J. Wall, Govt

Photolithographer, Adelaide, 1960),

MARSUPIALS: Macropodidae; Sthenurus gilli.

Alphabetical index to sites

Gawler 52.

Glencoe 66a.

Goolwa 61.

Goyder’s Lagoon 6,

Green Bluff Locality 7d.

Green Waterhole 66b.

Hallett Cove 58.

Haystall Cave 64f.

Henschke’s Bone Dig 63a.

Hergott Springs 13.

Hillpara Creek 27.

Hog Bay River 49.

Hookina Creek 19.

Innamincka 8.

James’ Quarry Cave 63b.

Kapunda 50.

Katpiri Waterhole 11i.

Kelly Hill Caves 47.

Kingston S.E. 62.

Kirkaldy Pit 57e.

Kyancutta 4.

Lake Callabonna 16.

Lake Fowler 44.

Lake Kanunka 10a.

Lake Palankarinna 12.

Lookout Locality 7e.

Mairs Cave 23.

Malkuni Waterhole 1 If.

Manunda Creek 31.

Marcus Locality 7c.

Marree 13.

Millicent 66c.

Moorak 67d.

Morgan 41.

Mount Burr Cave 66d.

Mount Eyre 20,

Mount Gambier 67.

Mount Taylor Cave 48a.

Mullett Locality 12b.

Murnpeowie 15.

Murrapaterinna 10b.

Naracoorte 63.

Naracoorte Caves 64.

Nectar Brook 28.

Newikie Creek 36.

New Kalamurina 7b.

Normanville 60a.

Pandie Pandie 5.

Peake 9,

Pekina Creek 29.

Penola 65.

Pernatty Lagoon 18.

Pondalowie Bay 45.

Pt Pirie Gravel Pit 32.

Punkrakadarinna Soakage 7f.

Reedy Creek 62.

Rocky River 46.

Salt Creek 60a.

Seton Rock Shelter 48d.

Specimen Cave 64g.

Tankstand Cave 68.

Tantanoola Cave 66e.

Teetulpa 24.

Thebarton 57f.

Tomato-Stick Cave 64h.

Town Cave 43a.

Two Wells 51.

Ulooloo 34.

Unkumilka Waterhole 1 1b.

Victoria Fossil Cave 641.

Warburton River 7.

Waupunya Creek 33.

Weekes Cave 1.

Welcome Springs 14.

Willochra Creek 21.

Yalpara Station 27.

Yankalilla 60b.

Yatala 53.

Note added in proof.

More detailed lists of fossil birds are to be

found in P. V. Rich (1975) Antarctic dispersal

routes, wandering continents and the origin of

Australia’s non-passeriform avifauna. Mem. Nat.

Mus. Vict. 36, 63-126.

Id D, -, G. WILLIAMS

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S. Aust, 95, 185-98.

—— (1972) Small fossil vertebriites from Vic-

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(Marsupialla), (bid. 96, 125-37-

—— (1976) Small fossil vertebrates from Wie-

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—— & Yinrz. A, H.C. (1896) Preliminary notes

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STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF THE BILLY

CREEK FORMATION (CAMBRIAN), EAST OF THE FLINDERS RANGES,

SOUTH AUSTRALIA

BY P. S. MOORE

Summary

Two new members (the Coads Hill Member and the Erudina Siltsone Member) are defined in the

Billy Creek Formation at Reaphook Hill. The Coads Member consists of a complex sequence of

shale, sandstone, carbonate and tuff which was deposited mainly in a shallow marine environment.

The overlying Erudina Siltstone Member consists of a silty and sandy redbed sequence with minor

dolomite and was deposited on tidal mudflats during a period of regression. A tentative correlation

of the Billy Creek Formation between Reaphook Hill and the type section in the Wirrealpa Basin is

suggested. The Billy Creek Formation also occurs in the Yalkalpo 2 well, east of Lake Frome,

where it comprises mainly green shales and sandstones. Deposition most probably occurred in a

relatively open marine environment, which suggests that the Arrowie Basin extended for a

considerable distance east of the present Flinders Ranges in the late Early Cambrian. The Billy

Creek Formation in the Lake Frome wells Nos 1 and 2, south of Lake Frome, considts of shaly and

silty redbeds with common anhydrite, and was deposited on high tidal mudflats laterally adjacent to

detaic sediments of the Eregunda Sandstone Member.

STRATIGRAPHY AND DEPOSITIONAL ENVIRONMENTS OF

THE BILLY CREEK FORMATION (CAMBRIAN),

EAST OF THE FLINDERS RANGES, SOUTH AUSTRALIA

by P. S. Moore*

Summary

Moort, PS, (1980) Stratigraphy and depositional environments of the Billy Creek Formation

(Cambrian). east of ihe Flinders Ranges, South Australia, Trans. R. Yoo. S$. Alust, 14(5),

117-132, 28 November, 1950.

Two pew members (the Coads Hill Member and the Erudina Siltstone Member) are

defined in the Billy Creek Formation at Reaphook Hill. The Coads Hill Member consists of

a complex sequence of shale, sandstone, curbonale and lui which was deposited mainly ina

shallow marine environment, The overlying Eradina Siltstone Member consists of a silty and

sandy redbed sequence with minor dolomite and was deposited on tidal mudflats during a

period of regression, A tentative correlation of the Billy Creek Formation between Reaphook

Hill and the type section in the Wirrealpa Basin is suggested. The Billy Creek Formation also

sceurs in the Yalkalpo 2 well, east of Lake Frome, where it comprises muinly green shales and

sandstones. Deposition most probably occurred in a relunvely open marine environment, which

suggests (hat the Arrowie Basin extended for a constderable distance cast of the present

Flinders Ranges in the late Early Cambrian, The Billy Creek Formation in the Lake Frome

wells Nos | und 2, south of Lake Frome, consists of shaly and silty redbeds with common

anhydrite, and was deposited on high tidal mudfluts laterally adjacent ta detaic sediments of

the Bregunda Sandstone Member.

Introduction

The Billy Creek Formation consists of an

Early to Middle Cambrian, predominantly

redbed sequence of shale, siltstone and sanc-

stone, with minor limestone, dolomite and tuff.

It crops out sporadically throughout the central

und northern Flinders Ranges of S.A., and has

been identified in the subsurface below the

Cainozoie and Mesozoic of the L. Frome

region (Fig. 1).

The Billy Creek Formation was formally

defined by Daily (1956), Outcrops in the

central and northern Flinders Ranges have

recently been subdivided into three members

by Moore (1979b). after redefinition of the

status of the Edeowie Limestone Member

(Moore 19794). However, these three mem-

bers are not recognised at Reaphook Hill or in

the subsurface oecurrences to the east of the

Flinders Ranges, due to the very individual

wature of the sequences, This paper discusses

the stratigraphy and depositional environments

of the Billy Creek Formation at Reaphook Hill,

and also briefly discusses the subsurface duta,

gathered primarily from the Yalkalpo 2 bore-

core, to the east of L, Frome.

The Reaphook Hill Outerop

The Billy Creck Formation at Reaphook

Hill is subdivided into two members. hereih

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Ranges and L. Frome Embayrment.

termed the Coads Hill Member and the Eru-

dina Siltstone Member (Fig. 2). The lower

sandy partion of the sequence (the Coads Hill

Member) was originally considered to be part

of the Hawker Group, comprising Bunkers

Sandstone equivalent and Oraparinna Shale

(Dalgarno & Johnson 1963), However, Dal-

garno (1964) recognised tuffaceous and red

Ls PS, MOORE

Reaphook

4 Hy ll

Erudina Siltstone

Member

“| Goads Hi)!

Member

NM Wilkawillitna

Ps Limestone

Pig. 2, Ourcrop nmap and locution of measured

stratigruphic sections, Billy Creek Pormation,

Reuphook Hill.

Rec setratigraphic

Coon ce ction

ee Fault

Billy. Creek

Formation

Geological

boundary

So Creek ‘ea

silty intervals in the sequence, and redefincel

it as part of the Billy Creek Forjnation, as

shown on the PARACHILNA 1:250 000 geo-

logical sheet (Dalgarno & Johnson 1966).

The upper part of the Billy Creek Formation

at Reaphook Hill (the Erudina Siltstone

Member) is dominated by silty redbeds, with

minor dolomitic atid sandy intervals.

The Reaphook Hill region was mapped in

detail in 197) by Gaunt! and Gehling?. Their

discovery of Emuellid trilobites in che lower

portion af the Billy Creek Formation is of

1Gaunt G. FM. (1971) The geology of the

Kempes Bore urea, eastern Flinders Ranges.

B.Sc. (Huns.) thesis, University of Avelaide

(unpublished }

> Gehling, J. G. (1971) The geology of the Reap-

hook Hill area. Flinders Ranges, South Australis,

B.Sc. (Hons) thesis, University of Adeluide

Uinpublished).

particular interest and the author is indebted

fo these two authors, whase work provides the

basis of the subdivisions presented below,

Stratigraphy of the Coads Hill Member

Introduction

The lower part of the Billy Creek Forma.

tian at Reaphook Hill comprises a sequence of

interbedded, fine to medium-grajined, pale

brown sandstone, dark grey limestone, and

minor red and green shale and shaly sillstone.

Interbeds of calcareous shale, shaly limestone,

dolomite and tuff occur in some units, and a

limestone-boulder conglomerate occurs at the

base of the sequence in the northern outcrops

(Fig. 3), The sequence is herein termed the

Coads Hill Member. The name is derived from

“Coads Hill” which is located approximately

7 km W of Reaphook Hill, Seclion RH-C

is chosen as the type section (Fig. 4).

The hase of the Coads Hill Member

In the north of the Reaphook Hill regian,

the basal 6 m of the Coads Hill Member com-

prise boulder conglomerate, with clasts of

Imestone wp to 30 cm across. The con-

glomerate was mapped as part of the under-

lying Hawker Group by Gebling*, hawever

it rests sharply and uncooformably on pale

grey, fenestral and oolitie Wilkawillina Lime-

stone. Further south, calcareous sandstones and

siltstones af the Coads Hill Member rest clis-

conformably on the Wilkawillina Limestone

(Figs 3 & Sa), A pisolitic calerete horizon,

5-20 ern thick, caps the disconformity surface,

Internal Stratigraphy

The Coads Hill Member is divided into mne

units (Fig. 3), which are deseribed belaw-

Units B to G are essentially the same as unils

recognised by Gaunt! and Gchling®.

Unit A is the basal unit of the Coads Hill

Member in the rorth of the Reaphook Hill

renion. TL comprises cobble to boulder coo-

glomerate, with clasts of pale grey, micritic,

fenestral and oolitic limestone and dolomitic

limestone, up to 30 cm across, The conglo-

merate has a closed fabric, with the matrix

comprising medium to yery coarse sand-sized

quartz and minor carbonate. Clasts are gene-

rally subangular to subrounded. Some are

fossiliterous, containing unidentified fragments

of trilobites and other shelly debris. The clast

lithologies are very similar to underlying Wilka-

willina Limestone

BILLY CREEK FORMATION EAST OF FLINDERS RANGES

Ed fark grey limestone Minor dolomite

Dark arey calcareous siltstone & sity |imestone

Shate imostly green) with calcareous interbeds,

Red, clayey sandstone and clayey selistoang, Minor srale,

Reddish brown taltareous sanastone, Minor shaly intecbeds

herizontal

Scale

Grey, limestone rich, cobble fo houlder congiemerate

Fig. 3. Stratigraphy of Coads Hill Member, Billy Creek Formation, Reaphook Hill.

Unit B is the basal unit of the Coads Hill

Member in the south of the Reaphook Hill

region, and conformably overlies Unit A in the

north, If comprises pale red to reddish brown,

fine to medium grained, feldspathic sandstone

(Fig, 5b). Interbeds of greyish red shale and

shaly siltstone are common in the upper por-

tions of the unit, The sequence is evenly bedded

to ripple laminated on the scale 3-15 cm.

Small to medium seale tabular cross-stratifica-

tian is common in the thicker sections, Desic-

cation cracks, symmetrical ripples, mudstone

intraclasts and small scour-and-fill structures

are common throughout the unit and worm

hurrows, interference ripples and pebbly hori-

zons occur in some outcrops. A 5 cm thick,

bright green tuffaceous interval with devilri-

fied shards occurs in the middle portian of

Section RH-H, in the north of the area,

Unit C comprises greyish red, very poorly

sorted, shaly siltstone to silty sandstone, with

minor granule and pebble-rich bands (Fig.

Sec). Ripple laminated interbeds of moderately

sorted, reddish brown sandstone, 5-20 cm thick,

are common in the lower portion of the

sequence, and define a passage from Unit B.

Mudstone intraclasts and desiccation cracks are

abundant (Fig. 5d). Bedding is poorly defined

in most of the unit, although the upper few

metres are dominated by red silty shale with

well developed, even lamination,

Unit D comprises a thin tongue of pale

yellowish brown, moderately sorted to well

sorted, feldspathic sandstone (Fig 3Se) which

crops out in the southern portion of the area,

where it resis conformably on Unit C (Fig.

3). The sandstones are evenly bedded on the

scale of 3-12 em with some poorly defined

ripple laminations and rare symmetrical tipple

marks, Large scale cross-stratification is absent.

A thin, bright olive green tuffaccous mterval

crops out in the upper portion of the unit in

12) r § MOORK

Section RH-G Green shale intraclasts and

incipient shrinkage cracks wre abundant

throughout the sequence.

Unit B is a sequenee of dark grey, foetid,

silty limestone, caleareous shale and siltstone

(Fig, Sf), In the thicker sections, a well-

developed sequence ranges from buflf-coloured

stromatolitic dolomite at the base, through

burrow-mottled shaly grey limestone and cal-

vareous shale in the lower portion, into dark

grey foctid limestone in the middle and upper

portion. Much of Unit E is bioturbated, and

desiccation cracks occur sporadically through-

our the sequence,

Unit F comprises pale reddish brown to

brown, fine fo medium-grained, feldspathic

sandstone. Interbeds of shale and siltstone are

common in some oulerops. Several bright

olive green tuffaccous intervals up to 30 em in

thickness are present, and are particularly pro-

minent in the wpper shaly portion of the umit.

The sequence is generally evenly bedded to

ripple laminated. Wowever, medium = seale

tabular cross-stratification is Common an the

60 northern outcrops (Fig. Sg). Mud-cracks,

— yuurtz-lined geades, oscillation ripples, current

ripples, mudstone intraclusts, small scour-and-

40 fill structures and worm burraws are common

throughour. Interference ripples occur in some

outcrops, In the north, the sandstones are

relatively mature, and are partly cemented

20 by calcite. Further south, the sandstones are

z interbedded with red shale and siltstone, and

contain rare pebble beds,

Unit G comprises green shale und calcy-

reous shale, with common, thin interbeds of

shaly, dolomitic limestone and dolomite.

Minor red shaly intervals oceur in the lower

portion of the unit, especially in the south,

Bright olive green tuffaceous interhéds, rarcly

up io 1.4m thick, are common throughout the

Type section (RH-C) of Coads Hill Mem- S¢4uenee. Units are generally evenly laminates,

. Billy Creek Formation. See legend Fix 8 although rare asymmetrical ripple marks are

Medion

very

toarse

Wilkawillina

woh

Fig

Fig. 5: a. Red shaly siltstones and sandstones of Unit B, Coads Hill Member, draping irregular discon-

formity surface al top of Wilkawillina Limestone. Hammer: 3] cm Jong. Location: Section RHC,

Reaphook Hill, b. Evenly bedded to cross-siratitied reddish brown siltstones and sandstones of Unil

B, Coads Hill Member. Hommer: 3) cm long. Location: Section RH-D, Reaphook Hill. c. Small

sundy channel in very poorly socted red shaly siltstone of Unit C, Couds Hill Member, Scale: 34

mm diumeter. Location: Section RH-A, Reaphook Hill. d. Incipient shrinkage cracks in fine red sand-

stone of Unit D, Coads Hill Member. Scale; 54 mm diameter, e Typical outcrop of Unit D, Couds

Hill Member, showing prominent ridge of evenly bedded and rarely. ripple Jaminated, mediur

grained satidstone. Locatian: Section RH-A, Reaphook Hill, f. Prominent ridge of grey, fuetid, silty

limestone and culeareous siltstone. Basal unit is lighter°coloured and dolomitic. Location: Unit &,

Conds Hill Member. Section RH-E, Reaphook Will. g. Cross-strutifieation in reddish brown cal

carcous sandstones of Unit Fy Coads Hill Member Note pbundance of mudstone intraclasts con-

conlrated on foresels of cross-strata. Location: Sevtion RH-F, Reaphook Hill, h. Basal view of

yellowish brown shaly dolomite containing abundant halite casts, Scale: 54 mm diameter. Location:

Unit H, Coads Hill Member. Section RH-C, Reaphook Hill.

BILLY CREEK FORMATION EAST OF FLINDERS RANGES 121

122 P. S. MOORE

a pes TY

BILLY CREEK FORMATION EAST OF FLINDERS RANGES |23

present in-sitty intervals in the south. Desic-

cation cracks and halite impriatts are econmen

in some sections (Fig. Sh), Abundant trilobites

(Baleoracania dailyi Pocock) and rare; uniden-

tified bracthopod fragments are present in

green Shale overlying dolomite, approximately

43 m above the base of Unit G in Sechoan

RH-A.

Unit H comprises 2 sequence dominated by

dark grey, foetid limestone, Interbeds of shily

limestune are enmmmon, and much of the se-

quence has 9 well-developed nodular (letsoid)

texture (Pig, 6a). The upper and lower par-

tions of Cinit Hoare shaly and dolomitic, and

contain stromatolites (Pig. 6b), desiccation

cracks and Ininor halite imprints. Unidentified

trilobite fragnents are uncommean, but huve

heen recarded From the middle to Upper por-

tien of the sequence

Unit J comprises approximately 3 m_ of

every laminated, khaki shale and tine siltstone,

with minor carbonate bands and nodules, The

trdobite B. deilyé is abundant in the basal

portion, anid is assaciated with care, unidepti-

fied brachiopod fragments. A 0.5 m_ thick

peloidal und aleal, mottled limestone forms a

prominent marker at the top of Unit J,

Age and Palaeontology

Trilobite traeks, worm burrows and mol-

luscan trails oceur sporadically throughout the

Couils Hill Member. At least one type of trace

fossil is present in every unit, with the excep-

tion of Unit C, Emvellid trilobites were first

discovered by Gaunt? and Gehling® in what

is now defined as the basal portion of Unit J

of the Cowds Hill Member, B, Daily (pers,

com jt Gehling’. p. 16) identified the trilo-

bites as B. dati. The species alsa oceurs in the

upper partion af the White Point Conglomerate

on Kangaroo Tsland, where it has been assigned

a late Barly Cambrian age (Pocock 1970),

Depositignal environitent of the Coads Hill

Member

Following deposition of shallow marine

and stpratidal carbonates of the uppermost

Hawker Group. the Adelaide “Geosyneline” in

the vicinity of Reaphook Hill was uplifted and

the Hawker Group eroded. Deposition of the

Coads Hill Member of the Billy Creek Forma-

Lion commenved when the area once again be-

came submerged. Limestone boulders eroded

from nearby areas were deposited in a near-

shore marine environment io the north (Unit

A) while a thin calerete profile developed on

the land surface to the south. Subsequently,

a sequence of shallow murine to intertidal,

caleareous sandstones (Unit B) spread over the

area,

Red, shaly and pebbly sandstones (Unit C)

are considered to be non-marine in origin.

because of a lack of fossils and their traces,

and also the extremely poor sediment-sorting.

Thus, a likely environment of deposition for

Unit © is a muddy alluvial plain, and its

presence in the Reaphoak Hill area indicates

a period of marked local regression.

The origin of the lower, foetid, shaly car-

bonute (Unit B) is of particular interest, since

it is underlain by redbeds which are probably

non-marine (Unit CY, and overlain by shallow

marine to intertidal calcareous sandstones

(Unit F). The lamination and fine grain-size

of Unit E indicates depositian from suspension

in a low energy environment. The lack of body

fossils Sugeests restricted marine conditions,

while the presefree of laminated dolomicrite,

Fie. 6; 9. Nodular (leno), shaly limestones of Unit H, Coads Hill Member, Hammer: 31 ¢m

long. Location: Secrion RH-H, Reaphook Hill b. Interbedded grey calcareous shale aud shaly lime-

stone of Unit HW, Conds Hill Member, Note presenve of weathered-out stromutolites in centre of

photo. Stromatolilte elongation perpendicular 1o outwrop. Hammer 31 cin Tons, Location: Section

RH-F, Reaphook Hill. c. Lurge sealy shuly-curbonate cycle in Unit A. Ertdina Siltstone Member. Red

shales pass grudationally through green shiiles and greyish green calcareous shiles into pule grey

to hyi-caloured dolomftic limestone. Rapid regression buck into red shale is vpical of cycles. Ham-

mer: J} cm long, Location: Section RH-C, Reaphook Hill. d. Thin unit of vellowish brown shaly

dolomite with wavy stromatolitic laminations in niiddle of asymmetrical shale-dolomite-shale cycle.

Scate; 54 mm diameter. Location: Unit A, Erudina Siltstone Member, Section RH-C, Reaphook Hill,

ce Wovy and Jenticulur bedding in shaly siltstones of Unit D, Erudina Siftstone Member, Mudfinke in-

trackisrs are common, Location: Section RH-C, Reuphook Hill. f. Current linented red micaceous

sundscones of Unit C. Erudina Sillstone Member, Scole: 54 mm diameter. Location: Section RH-C.

Reaphook Hill 2. Large lood slirictures with subvertical syfometry, probably associated with

Jewalering. Hammer: 31 em lone Location: Unil ©, Briudina Siltstone Meniber, Section RH-C,

Renphook Hill. bh. Semimetrical wave ripples in coarse red silfstone. Bedding surface dissected by.

large, palvgonul desiceation chucks inflled with red mudstone, Lenscup scule: 54 mm diameter,

Location: Section RH-C. Reaphaok Hr).

124 P. S. MOORE

top Aot exposed

MEMBER

—_

—

—!

ERUO |

medium

very

Coads Hill

sno}

Fig. 7. Type section (RH-C) of Erudina Siltstone

Member, Billy Creck Formation, Reaphook

Hill, See legend Fig, &.

stromatolites and desiccation cracks indicates

that af Jeast part of the sequence Was deposited

in shallow water, The foetid odour and dark

colour of the bulk of Unit E is evidence for

restricted circulation and poor oxygenation,

such as occurs in a restricted embayment or

lagoon. Unit D sandstones, which are laterally

equivalent to Unit E, probably represent de-

position in a littoral environment

Shallow marine calearcous sandstones of

Unit F pass gradationally into micaceous

shales of Unit G, The shales contain arthropod

tracks and dolomitic intervals, and thus were

Jeposited on subtidal to intertidal mudtlats

subject to frequent marine inundation and

reducing conditions,

The upper, dark, foetid limestone (Unit H)

is somewhat different from the lower one, for

it contains minimal terrigenous clastic detritus,

and is relatively uniform in thickness and

character throughout the area of outerop,

Thus, Unit H probably accumulated in a semi-

restricted, very shallow marine environment,

subject lo only minor fine-grained terrigenous

influx. A coanection with the open sea is in-

ferred from the presence of trilobites, however

the water was generally quite shallow, as indi-

cated by sporadic desiccation cracks and

stromatolitic intervals, and was also poorly

oxygenated, as indicated by the high organic

eontent of the limestone, its dark colour and

its foetid odour.

The thin sequence of green fossiliferous

shale (Unit J) which occurs at the top of the

Coads Hill Member indicates a period of fine-

grained clastic deposition in a relatively open,

shallow marine environment, A rapid decrease

in fossil fragments towards the top of the unit

indicates progressive restriction and shaflowing

of the basin, prior to the deposition of the

Erudina Siltstone Member.

Stratigraphy of the Erudina Siltstone Member

fatroduction

The upper portion of the Billy Creek For-

mation at Reaphook Hill comprises a sequence

of greyish red siltstones and silty shales, with

minor dolomitic, tuffaceous and sandy iiter-

beds. The sequence is herein termed the Eru-

dina Siltstone Member, The name is derived

from the Erudina homestead, located approxi-

malely 15 km SE of Reaphook Hill.

The Erudina Siltstone Member crops out i

the central portion of a small basinal structure

at Reaphook Hill (Fig. 2), where it conform.

ably overlies the Coads Hill Member, Maxi-

mum measured thickness is 270 m in Section

RH-C, however the original thickness is un-

known since the upper portion of the member

has been removed by erosion, Section RH-C

as chosen as the type section (Fig. 7), The

member is clearly divisible inty four units,

described helow,

BILLY CREEK FORMATION EAST GF FLINDERS RANGES \25

Internal Stratigraphy

The basal unit of the Erudina Siltstone

Member (Unit A) comprises a fine-gcained

sequence of cyclically interbedded silty shale

and carbonale. Halt-cycles, from red shale

through pale greyish green shale info buf

coloured dolomite or dolomitic limestone are

typical (Fig. Ge). The carbonates are cyenly

laminated to wavy laminated, with rare desic-

cation cracks, hahte imprints and stromatolites

(Fig. Gd). Shaly and silty clastic intervals

commonly contain desiccation cracks and

symmetrical ripple marks, Raindrop imprints.

calcareous algal mats, halite imprints, worm

burrows and arthropod tracks and trails are

rare,

Unit B comprises approximately 80 m of red

shale. silty shale and shaly siltstone, with

minor sandy interbeds. The sequence is evenly

laminaled, with minor wavy bedding (Fig. 6e)

and ripple lamination in the coarser units.

Symmetrical and near-symmetncal (wave-

formed) ripples predominate, although highly

asymmetrical (current formed) intetference

ripples, and flat-topped ripples also occur.

Desiceation cracks and mudstone intraclasts

are abundant, whereas halite casts and small

load structures are relatively uncommon. The

redbeds are Weakly calcareous, and crenulated,

carbonale-rich algal mats occur in a few lovali-

ties, Arthrapod tracks and biotucbated inter-

vals are rare. Pink. silty, tuffaceous units ate

also rare,

Unit C comprises a 40 m thick sequence

ol interbedded shaly, silty, and sandy redbeds.

Coarsening-upward cycles are present, and vary

in thickness from a few metres to twenty

metres. The silty units are wavy bedded to

ripple laminated, and are commonly associated

with desiccation cracks, mudstone intraclasts,

trilobite tracks, worm burrows, and symmet-

rical interference and current ripples. Sandy

intervals are commonly ripple laminated, with

rib-and-furrow structures on the upper surface.

Thicker intervals in the upper portion of Unit

hake Frome Se ae

wells

C are horizontally laminated, with well-

developed current lineation (Pig. 6f), current

crescents and rare bounce marks. Trilobite

tracks and scratch marks are common in the

sandy nits, which also contain desiccation

cracks, mudstane intraclasts, load structures

(Fig, 62), rare worm burrows. and molluscan

trails.

Unit D comprises a 100 m thick sequence of

interbedded red silty stiale, shaly siltstone and

silislone very similar in character to Unit B.

Silty intervals ure wavy bedded, flaser bedded,

and ripple laminated, and both symmetrical

and asymmetrical ripple marks are abundant

throughout the sequence (Fig. 6h). Desicca-

tion cracks, halite imprints. and mudstone intra-

clasts are common. A few units contain inter-

ference and flat-topped ripples.

Palaeonfalney

Worm burrows, molluscan trails and tracks

attributed to trilobites occur sporadically

throughout the Erudina Siltstone Member. The

only body fossils found to date are tiny (1-2

mm long) carbonaceous imprints in green

shale in the lower portion of Unit A. These

are interpreted as fossil annelids.

Depositional environment of the Erudina

Siltstone Member

The Erudina Silistane Member consists of

four units which are distinguished primarily

on the basis of grain-size, Unit A is fine-

grained, comprising red shale with dolomtic

interbeds. The shales were deposited in an

oxidising environment on muddy tidal fats

probably as a response to mild tectonism (the

Kangarooian Movements of Daily & Forbes

1969). Carbonate mudstones accumulated in

the lower intertidal to subtidal environment

during periods of relative tectonic quiescence.

Cycles in the shale-carbonate sequence of

Unit A are attributed to local transgressions

and regressions, and reflect the unstable nature

of the basin of deposition and adjacent source

areas during this period,

Mount

Arrowsmich

sea level

-sbom

-1ooom

-1500m

Fig, 8. Simplified cross-section, castern Arrawie Basin, See Fig | for location and legend.

126

Unit B was deposited in response to in-

creased tectonic activity, whereby red shales

and siltstones were deposited on muddy inter-

tidal flats and in the shallow subtidal environ-

ment. The rate of sedimentation was sufliciert

to obscure carbonate accumulation and in-

stead, a sequence of fine-grained redheds with

distinctive tidal stratification (cf. Reineck &

Wunderlich 1968) was developeu..

During the deposition of Unit C, sand was

carried into the basin, forming coarsening-

upward cycles of redbed clastics. The eycles

are attributed to pulses of tectonise which

reached a peak late in the history of deposition

of Unit C. Unit D represents a return to same-

what more stable conditions, as experieticed

during the evolution of Unit B. Fine-pgramed,

shaly and silly redbeds dominate the sequence,

which contains an abundance of poorly defined

simple and wavy flaser bedding.

Subsurface distribution of the Billy Creek

Formation

The Billy Creek Formation occurs sub-

surface in the Arrowie Basin to the east of the

Flinders Ranges, wenerally below the Mesozoic

of the L. Frome Embayment and in some

places below the Cainozoie of the Tarkaroo-

low Basin®, The present limits of the Cambrian

basin in this region, as suggested by Youngs',

are shown in Figure 1. A simplified cross-

section is presented in Figure 8.

* Osborne first introduced the tern “Frome Em-

buyment’ defining it as a aynelinal basin

bounded by (he Flinders und Barrier Ranges, As

presenuly defined (Wopfner 1969). the term

‘Frome Embayment" refers only to the Mesazoic

sedimentary basin. The overlying Ciuinozaic

sediments of the Tatkaroolod Basin! are ungon-

Formuble an the Cretaceous and relute lo u dif-

ferent cycle of events.

Youngs, BC. (1969) Bumburlow |—well com-

pletion report, S. Ausi. Dept Mines & Energy

(unpublished )-

Osborne. N. (1945) Report on ail and gas pos-

sibilities of the Frome Embaoyment, New South

Wales and South Australia, for Zine Corp. Ld.

8. Aust. Dept Mines & Energy open file report

(unpublished).

Callen, R.A. (1976) 1,250 000 geologieal series

explanatory poles, FROME, South Australia.

S, Aust. Dept. Mines & Energy Rept 74/27

funpublistied }.

* Dethi Australin Petroleum bid, and Santos Lid

(1969) Well completion report, Lake Frome

1, 2 & 3, 8S. Aust. Depr Mines & Energy open

‘ile envelope 968 tunpublished),

“Youngs. B.C, (1977) Mudguard t and Yalkalpu

2—well completion reports. S. Aust. Dept

Mines & Energy 77/66 (unpublished).

PS MOORE

As shown in Figure 8, the Billy Creek For-

mation was intersected by L, Frome strati-

graphic wells Nos, | & 2% and SADME Yal-

kalpo No, 2% The EAR uranium exploration

holes south of L. Frome mostly ended in

weathered and leached, shaly redbeds®, many

of which probably belong to the Billy Creek

Formation. An interpretive subcrop map for

the area south of L, Frame is presented in

Figure 9, hased on ihe aufhar’s own evaluation

of cores and cuttings.

SADM Yalkalpa No. 2

The Billy Creek Formation in Yalkalpo 2

comprises red and green shales and sillstones,

with common reddish brown sandy intervals*.

Approximately 265 m of strata attributed to

the lower portion of the Billy Creck Formation

were intersected (Pig. 10), The original total

thickness of the formation at this locality is un-

known, since the Upper portion of the sequence

has been removed by post-Cambrian, pre-

Cretaceous erosion (Youngs 1978),

Feat oe

rey)

Precambren ceystadine

BS hassmnnt

POLARY aboce

cen SS gy ¢

¢ ‘5 bg :

Tertiary and Quaternary

strata

| i ireeh FY Mation

Fa > bate Precambs sah and

“oe stay Gambrien strata

{i SH esa rete ny St 2\ ene

al sasement “yo DS

Fig. 9, Interpretive preCretaccous subcrap mup..

south of Lo Frome, Evidence suggesis only

thin pro-Billy Creek Formation clastic sequence

in this area. with probable faulting against

Olary Block.

—— Geologic eoundaty

—— Faull | ntlerrec!

wt Leke Frome writ

+ FA Ragd welis

™ Giece Dak Wore

BILLY CREEK FORMATION EAST OF FLINDERS RANGES

A moderate to high sand content, and a

dominance of nan-red sediments differentiates

the Yalkalpu 2 sequence from most other

known occurrences of the Billy Creek Forma-

tion, and the absence of carbonates differen-

liates it from the Caads Hill Member, Thus,

the Yalkalpo 2 sequence between 258 m and

523 m depth is defined as. Billy Creek Forma-

lian sensu sirieta.

Fine-grained intervals dominate the se-

quence, particulafly in the upper portions, “A

faeies spectrum is present, from ripple

laminated fine-grained sandstone wih green

shale Nasers, through wavy flaser and lenticu-

lar bedded units (ef. Reineck & Wunderlich

1968, and Reineck & Sinuh 1975) into evenly

Jaminated green shale (Fig. 10), Redbeds com-

prise only abaut 30% of the fine-grained

association and generally consists of wavy

bedded to evenly laminated shales and

coarse siltstones, Worm burrows are common,

and oceur mainly in the green intervals. Mol-

luscan trails and tracks attributed to trilobites

occur both in red and green coloured sediment,

although they are slightly more common in

the latter. Desiccation cracks are abundant in

many of the red shale intervals, and in rare

cases are ussociated with halite imprints. and

patches and veins of anhydrite, Cyclic sedi-

mentation between red and green intervals,

each with its characteristic set of sedimentary

structures and organic markings, is a feature

of the middle portion of the sequence

(especially in the intervals 380-450 m).

Coarse-grained intervals comprise reddish

brown to yellowish brown, very fine to

medium-grained feldspathic sandstone, In

some cuses (e.g. at 497 m) the sandstones rest

sharply on fine-grained sediments, and contain

wbundant mudstone intraclasts in the basal por-

tions of the units. More commonly however,

the sandstones oceur at the top of coarsening-

Rudd, B.A. Pry Lid (1970) Report on mvesliga-

tions, Take Frome Embaymenr, S.A. SMI’s 267

and 268. §. Aust. Dept Mines & Energy open

file envelopes 1109 & 4170 (unpublished).

W Daily, B. (1969) Remarks on the subsurface

strativraphy and palaeontalogsy of the Delhi-

Santos Lake Frome Nos 1-3 Stratigraphic Wells

5. Aust. Dept Mincs & Energy open file

envelope 968 Cunpublished )-

1) Moore, P_S. (1979) Stratigraphy and sediment

ology of the Billy Oreck Formation (Cambrian.

Flinders Ranges) and is equivalents on the

noriheast coast Of Kangaroo Island, South

Australia. Ph.D, thesis, University of Adelaide

Cunpublisheett,

L232

upward sequences, They are generally evenly

bedded, with abundant soft-sediment deforma-

tion i the thicker units. Some of the thinner

sandy units are ripple laminated. and green

und minor red flasers may be present, Mud-

stone intraclasts are common. A feature of the

sandy intervals is the absence of well-

developed large-scale cross-stratifieation.

Delhi-Santos Lake Frome Stratigraphic Wells

The Billy Creek Formation sensu stricto has

been identified from the L, Frame wells Nos.

lund 2 by Daily! This identification is con-

firmed here, Only the upper part of the Billy

Creek Formation was penetrated?, and this

interval is considered to be the approximate

lateral equivalent of the Eregunda Sandstone

Member in the central and nonhern Flinders

Runges (Moore 1979b), However, the interval

is not appreciably sandy and thus should not

be referred to as the Eregunda Sandstone

Member. Rather. it is considered only as

“Billy Creek Formation”.

A lox of the Billy Creek Formation as

intersected in L. Frome No. 1 is presented

in Figure 11. The sequence is rather homo-

genous, comprising fine-grained tedbeds with

Minor green intervals. A transition into the

the overlying Wirrealpa Limestone ts indi-

cated. Cullings were sampled at 10 feet inter-

Vals and cores 5-7 were taken in the Billy

Creek Formation (Fig, 11).

Examination of cored intervals reveals a

spectrum of facies, with increasing silt con-

tent. ranging from evenly laminated claystones,

through wavy bedded mudstanes, inta poorly-

defined flaser-bedded siltstones. Ripple lami-

nated siltstones devoid of clay laminae are

uncommon. Anhydrite and calcite patches,

veins and lenses are present in all cored

intervals, although they are more common in

the finer-grained facies. Secondary reduction,

ussaciated with a colour change fram red to

preen, commonly surrounds the anhydrite’,

Halite imprints oceur sporadically through-

out the cored sections, and typically occur on

rippled bedding surfaces. Desiccation cracks

are common. Mudstone intraciasts and rill

marks are also common in parts of sequence,

particularly in the coatser-grained intervals.

Thin, pinkish igtervale at 780.3 m and 780.7

m in core 7 of L. Frome No. 1 contain

abundant altered. subangular feldspar, and by

anglogy with outerops in the Flinders Ranges,

are considered ta be tuffaceous in origin.

uorjequaiso ajddis uoljeijioso 7%

Smollo) S® g PUR » SaunBi4 UI UWnIoD

au) jo apis puey yybin ayy

eyep yussinao0oe|ed

sjissoj Apog 4 s49e17 podosyyiy

S124] VEISNIIOW Afi SMO1ING WIOM Q

Sainjeay diuebio

FPIAB

UMOJg JOUIW YIM Pay dy ayapAyuy

umosq-Pay Jey sainpovopnasg 2

kaso 49 $aunqonsys peol a

vaas9 ug sjse2 ydsowopnasd aqieH Q

w UMOJg 48 sysej2esju! auoyspnw v

& pay 4 sy2es2 vorjed2Isag _AL

S INO|OD 4IOY sainjeaj Asequawipas

< c

A, oS Sint

a Sioa

@ are

i] wet

auoysyjis paiddis-quasin9

Buippaq saseiy aidwis

Buippaq Aaem

6ulppaq vasuid

a3112/Wo10g

auoysawi) 213/491W

=a] =~ 0

eel sSls

co po}eols

N e3)}cs fe

re) ae

= a a5

ania

Sjuasan> jeuolydasIplun a

siydesbiyesys

uo UMOUS aJe SjUaJIndOae|eYg

‘owmOLy “JT JO isva ‘7 odjeyyex ur

—saiqgad

dNO49 YSNMVH

PIWIOJUOISIPE

BBS

Bes SEAS

OES

02S

pO6Y

WOPP

—saiqgad

—pues

UOeULIOT YIeID Alig ‘soy s1ydeisNeNS ‘OT “By

ory ose

oer Ore

Ozr oee

Oly Loze

oor ole

vuby FOBE OoE

| —toee 062

Ooze O82

leasaqur pasos 40 doy WOO?

BILLY CREEK FORMATION BAST OF FLINDERS RANGES 129

Qrey moltied limeshone

and argiilateous limestone

‘|

petioles dls yraaayt Wh I,

lamfleted with minor wavy

agal taminge Rare cliibing

\ Tippime Annyurice pate hes

\ane reworked inti qeipscs,

>— Grey #ien minor ced shale &

Vie aredus SiILStOne, Evenly

Greyen Ten ann green onale

ano stestone With ver? Minor

Sandshine Passes qradat onaily

inte the overiying Werreaipa

Loamestone

/Greview rad and minge

/greer clalse Gillstone and

snale Evenly laminated ond

flaser bedded Lommon nhatite

\ SastS desigcation crachs,

abhydhif® ahd musstone

Ante aclasle

rore

teh lbhen

Uresien red and itioor green

Shale ano eri stone

1700m

Laswe’

e :

ean’

[Dreyen red ane mingr

Joven shale and fine to

| Mediu eitstone Evenly

‘laminated wort) mince tlaser

[arspny twalite casts,

parsaccarion erarks mudscone

Joyerartasts ane anhyatice

‘ga PS

Beotn

KB!

Fig. 11, Stratigraphic log, Billy Creek Formation

in L. Frome 1,8 of L. Frame-

Tracks attributed to trilobites occur in several

of the cores™, however no body fossils have

been found to date.

foternal correlations

The Pridina Siltstone Member at Reaphook

Hill is considered to be the approximate lateral

equivalent of the Nildottie Siltstone Member

in the central Flinders Ranges (Fig, 12)-

Roth members are interpreted as being the

result of a major phase of tectonism in the

source area which caused basin-wide regres-

sion and promoted the development of red-

bed facies over a wide area.

Similarities between the underlying Conds

Hill Member at Reaphook Hill and the Warra-

gee Member in the central Flinders Ranges

support this correlalion (Fig, 13), In the

Wirrealpa Basin type section, the upper part of

the Warragee Member comprises a semi-

restricted marine sequence with green shales,

several thick dolomite beds, and prominent

tulfaceous intervals. A comparable although

less-restricted sequence is present in the upper

portion of the Coads Hill Member (Units G-J)

at Reaphook Hill and a correlation is made on

this basis. In particular, Unit H of the Coads

Hill Member (an open marine, grey lime-

stone) is considered to pass laterally (shore-

wards) into a sequence of interbedded dolo-

mites and green calcareous shales in’ the

Wirréalpa Basin (Fig. 13). On the basis of this

correlation, it would appear that the strata

containing B. daily/ at Reaphook are essen-

tially the same age as those containing B.

flindersi in the Wirrealpa Basin (Fig. 13),

despite the appearance of B. flindersi in the

type section being partly controlled by sedi-

mentological cather than evolutionary factors

(Moore 1979b).

Correlation af the Billy Creek Formation

between Reaphook Hill and the central Flin-

ders Ranges has been made possible only by

the fortunate coexistence of distinctive tuffa-

ceous and calcareous sequences. Either of

these features on its Own would probably have

been insufficient for a satisfactory correlation,

It was hoped that a similar method could be

employed for the correlation of the Billy

Creek Formation between the outcrops of the

Flinders Ranges and the subsurface occut-

rences to the east, Unfortunately, neither thick

tuifs nor distinctive calcareous beds were

found in the Yalkalpo 2 borecore, and thus

the relationship between this sequence and the

rest of the Billy Creek Formation remains

uncertain, However, since there is no evidence

af a regression in the upper portion of the

Mee faite ae tS ~I NETS alee sean Ooh rit

SHON A .

— A eae

ior =

a wepmne

he \ MET Ne =

tay

Wyeie Ah

i > anys

tikanenl on — : _ Wha WAAL ed

et" > -nqpaeiubh cpr Mrs Lune

tm un }

or = —. 2 ol

Fiz. 12, Stratigraphy of Early to Middle Cambrian

Billy Creek Formation,

P. S. MOORE

Ten Mile Creek Reaphook Hill

Section BC-B Section RH-A

metres

Tuff (50cm) UNIT H ow

B. fFlindersi

300 Tuff (4m )—

Ww UNIT G

Bflindersi _|_ _ iii, seasityi

m Tuff (40cm) ge dally! =

pace ratte —_

Sarge al uw

= eat Ban eee Tuffaceous shale

2 Ri eat (15m) =

= 250 Suh dae eee

ee a UNIT G

ee ott

ld e u

oat

acre Vo

(10cm) ‘tos UNIT F

UNIT E

UNIT D

UNIT C

WwW

—

{e)

UNIT B O

<< x

te}

7 “ge {ty

4 ye vu

L x o- €

ao / o* o

joe

/ v= TUFF

/ Limestone

= /

J Dolomite

Shale and fine siltstone

= <

Rippled siltstone and sandstone

Evenly bedded sandstone

SSAARAARASS

SSS

S333

Cross bedded sandstone

BILLY CREEK FORMATION EAST OF FLINDERS RANGES (4)

preserved Yalkalpo 2 sequence corresponding

with the development of the Nildottie and

Erudina Siltstane Members further west, it is

likely ihat the Billy Creek Formation in Yal-

kalpo 2 is equivalent to the lower-middle and

upper parts of the Warragee and Coads Hill

Members,

On the basis of isopach and palaeocurrent

trends, Moore (1979¢) considered that the

Ereeunda Sandstone Member was originally

deposited st Reaphook Hill, but has since

been removed by erosion, The apparent ab-

sence of the Eregunda Sandstone Member in

the Delhi-Santos L. Frome wells (Fig, 11) is

interpreted as an effect of lateral facies change,

with deltaie sandstones passing laterally inra

supratidal evaporitic mudflats. A camparable

Recent example is quoted by Thampson (1968,

1975) from the Gulf of California.

Conclusions

In the northern part of the Adelaide “Geo-

syncline’, initial teetonie activity associated

with the Kangarovian Movements (Daily &

Forbes 1969) terminated a major phase of

Early Cambrian carbonate deposition and pro-

moted the development of 4 thick sequence of

red-beds (the Billy Creek Formation). Five

oiemhers are defined within the Billy Creck

Formation (Moore 1979b and this paper),

which crops out in the Flinders Ranges and

oecurs in the subsurface to the east, During

the varly stages of deposition of the Billy

Creek Formation, a broad muddy tidal flac

developed in the west (the Warragee Mem-

ber) while to the cast, a cornplex stratigraphy

(the Coads Hill Member) was evolving, The

great variely of facies in the Coads Hill

Member emphasises the instability of this

pastern region during the late Early Cam-

brian, althouch in general this sequence and the

laterally equivalent scquence in Yalkalpo 2

were deposited in a more open marifte environ-

ment than the Warragee Member, Minor

volcanic activity, probably in the ME Wright

region of N.S.W., is recorded as thin tullaccous

interbeds in the lower half af the formation.

Further uplifts in the source area released

silt and fine sand into the basin, forming the

laterally equivalent Nildottie and Erudina

Siltstone Members. The red-bed facies uf both

members were deposited mainly in the inter-

tidal to supratidal zones undec the influences

of weak wave and current aclivity. while

cyclically interbedded dolomites in the more

easterly outeropping Erudina Siltstone Mem-

ber were probably deposited in sheltered

coastal lagoons in the shallow subtidal zone,

Final uplift further increased topographic

relief in the source trea and a complex of

fluvial dominated fan-delta sands (the Ere-

gunda Sandstone Member) prograded across

(he basin of deposition from the southeast

(Moore 1979c), Palacocurrent and petro-

eraphic data indicate that the main source af

the sediment was the Broken Hill-Olary base-

ment high.

Acknowledgments

| acknowledge discussion and helpful criti-

cism by Dr B, Daily (University of Adetaide),

Dr T. J. Mount (Delhi Petroleum Pty Lid),

Dr G. Necf (W. 5, & L. B, Robmsan Univer-

sity College, Broken Hill}, and Messrs R.

Dalgarno, R. Callen and C. Gatehouse and

Miss B. Youngs (S Aust. Department of

Mines & Energy). The tolk of the work was

completed at the University af Adclaide during

the tenure of a Commonwealth Postgraduate

Scholarship, supervised by Dr Daily and sub-

mitted in extended form as x thesis dissertation

in June 1979. The revised manuscript is pub-

lished with the permission of Delhi Petroleum

Pty Ltd.

References

Daity, B. (1958) The Cambrian tn South Aus-

tralla. Jn J. Rodgers (Fd.), El sistema Cam-

brico, sti palacogeowrafia el problema de su

base, 200 Int. geol. Coner., Meriva, yal. 2, 91-

147.

& Forsrs, B. G. (1969) Notes on the Pro-

terozoic und Cambrian, southern and central

Flinders Ranges, South Australian, Jr B, Daily

(Ed), Geologieas! Excursions Handbook, 23-30.

ANZAAS, Section 3, 1969.

Daccaano, ©, R- (1964) Report on the Lower

Cambrian stratigraphy of the Flinders Ranges,

South Australia, Trans. R, Soc. S. Anst, BR 129-

144.

___ & Jonson, J. E. (1963) Lower Cambrian of

the enslern flunk of the Flinders Ranges. Quart,

cool. Notes, Goal. Surv. suet. 7.

— & Jonnson, §, E. 11966) PARACHILNA

map sheet, Gealogicnl Atlas of South Austraba

1-250 N00 series. Geol. Surv, S. bey?

Fig. 13. Correigtion of Billy Creek Formation between, Renphook Hill and iype section. in Wirrealpu

Basin. 2m (hick dolomite and overlying sequence of calcareous preet shales t Section, BO-B ute

correlated with grey murine limestone (Unit 1) al Reaphook Hill. Both writs are [ossiiiferous, con-

tainins trilobile Lalcorurunia sp. Although sequences ire Lu pceous,

corekuion of individual Tt

heds between oreas iy nol generally possible. und certninly not reliable.

132 P. S. MOORE

Moore, P. S. (1979a) Stratigraphy of the Early

Cambrian Edeowie Limestone Member, Flinders

Ranges, South Australia. Trans. R. Soc. S. Aust.

103, 101-111.

(1979b) Stratigraphy and depositional en-

vironments of the Billy Creek Formation (Cam-

brian), central and northern Flinders Ranges,

South Australia. Ibid. 103, 197-211.

—— (1979c) Deltaic sedimentation—Cambrian of

South Australia. J. Sedim. Petrol. 49, 1229-1244,

Pocock, K. J. (1970) The Emuellidae, a new

family of trilobite from the Lower Cambrian of

South Australia. Palaeontology 7, 458-471.

REINECK, H. E. & SinGu, I. B. (1975) “Deposi-

tional Sedimentary Environments with Refer-

ence to Terrigenous Clastics.” (Springer-Verlag:

New York.)

& WUNDERLICH, F. (1968) Classification and

origin of flaser and lenticular bedding. Sedi-

mentology 11, 99-104.

THOMPSON, R. W. (1968) Tidal flat sedimentation

on the Colorado River delta, northwestern Gulf

of California. Jn R. N. Ginsberg (Ed.), “Tidal

deposits: a casebook of Recent examples and

fossil counterparts.” (Springer-Verlag: New

York.)

Younas, B. C. (1978) Stratigraphic drilling in the

eastern Arrowie Basin, 1975-1976. Quart. geol.

Notes, Geol. Surv. S. Aust. 66, 16-20.

NEW ROTIFERA FROM AUSTRALIA

BY W. KOSTE & R. J. SHIEL

Summary

One hundred taxa of Rotifera, including six species: Lepadella chengalathi, L. williamsi, Lindia

deridderi Koste, 1979, Testudinella walkeri, Filinia australiensis Koste, 1980 and F. hofmanni

Koste, 1980 and five new subspecies are recorded from Australia for the first time. Eight new taxa

in the genera Brachionus, Keratella, Lepadella, Lecane, Dicranophorus and Testudinella are

redescribed and figured. Other species names, with ecological and locality information, are listed

systematically.

NEW ROTIFERA FROM AUSTRALIA

hy W. Kosre* & R, J. Swrery

Summary

Kogru, W. & Sten, Ro J (1980) New Rotifert. from Australia. Trans. R. Soe 5S. Aust. 405).

133-144, 28 November, 1980,

One hundred taxa of Rotifera, including six species: Lepadella chengalathi, L. willtamst,

Lindia devidderi Koste, 1979, Tesnulinella watkeri, Filinta wustraliensis Koste, 1980 and F.

hofmanni Koste, 1980 and five new subspecies are recorded fram Ausiralia for the fipst time.

Right new taxa in the genera Brachrows, Keratella, Lepudella, Lecane,

Dicranepharis and

Testudinella are desenbed and figured. Other species names, with ecological and Jocality infor-

mation. are listed systematically.

Introduction

Rotifera are found in virtually all inland

waters, They are usually the numerically

dominant component of the zooplankton of

lakes, rivers, billabongs and swamps, providing

an important link in aquatic food chains

between the nannoplankton (i.c. less than 60

nm, including bacteria snd micro-algae) and

the carnivoraus zooplankton.

Publication of the first checklist of the

Australian Rotifera (Shiel & Koste 1979)

and a review of the Australian species of

Brachionus and Keratella (Koste 1979) has

resulted in increased interest in the rotifer

fauna. Workers locally and averseas have com-

municated papers and collections, enabling the

faunal fist to he expanded. The first material

from the Northern Territory bas been

examined, and access has been provided to

collections from Tasmania and Weslern Aus-

tralia, Material from the other States has been

collected during a survey of the zooplankton

of the Murray-Darling system (Stel 1978,

1979),

Consequently, while this paper adds to the

known rotifer fauna of the continent, it Tmust

be considered as a preliminary to a more com-

prehensive treatment acu later date, in which

illustrated keys will be provided for assistance

in identifeation of the Australian Rotifera., At

present, taxonomie references in which many

of fhe cosmopolitan taxa are figured include

Barlos (1959), Kutikova (1970) and Kaoste

(1978), none of which is readily accessible to

the English-speaking Australian limmologist,

One hundred taxa of Rotifera are recorded

from Australia for the first time, In addition,

three species (Ascamerpha saltans, Pomphalyx

* Lucwie-Brill-Strasse 5, Quakenbruck, D570,

West Germany.

| Department of Zoology, University of Adelaide.

sulcata and Tesiudinella amphora) are recorded

by Sudzuki & Timms (1980) from farm

dams in N.S,W. These species were recorded

in the present study and are retained in the

listing to provide ecological information. Sud-

zuki & Timms’ record of Filinia maior is con-

sidered synonymous with F. terminalis (see

Koste 1978). A further three species described

by Berzins (1961) were omitted From the ori-

ginal checklist, and are included here, bringing

the recognised Rotifera taxa from Australia

to 437. In some cases, taxa having minor dif-

ferences from the type al the sub-specific or

varietal level are the only representatives of

the species recorded to date from the continent,

and are therefore included in the record as

distinct taxa follawing the principles of Mayr

(1969),

Although it would be premature to give de-

tailed ecological information on the collections,

particularly since material from large areas

af the continent has yet to be examined, we

include information on the habitats from which

the various taxa are recorded. The format

adopted is as follows;

All records are listed systematically (after

Koste 1978). Habitat type is indicated by:

L: lake or impoundment, with name of

locality;

R; river or Stream,

named;

B- billabong (standing waters on the flood-

plain), ‘with nearest town or setiiement

named,

The season of collection is. given as W:

winter: Sp; spring; Su> summer and A:

autumn,

Physico-chentical data js given in the

sequence: temperature in °C (measured with a

Yellow-Springs Instrument Company thermis-

tor); pH (Metrohm portable pH meter);

with nearest town

134

dissolved oxygen (YSI DO meter): turbidity

(Hach turbidimeter, or where a metric mea-

surement is given, by Secchi disc); conductivity

(Radiometer CDM2 conductivity meter). In

the example given below, the units of measure-

ment for each parameter are given in paren-

theses:

“Lecune stichaea Harring, 1913

Loc: R, Mannum, S.A., Wz 11.0 (°C), 8.4

(pH), 10.8

(DO in ppm), 40 (turbidiity in Nephelometric

Turbidity Units), 575 (4S cm),

Several species came from collections

other than by us, For these, physico-chemicyl

data were not available to us.

No distinction 1s made between planktome

and littoral species. Seasonal variation occurs,

particularly when billabong species are flushed

into rivers to constitute the plankton in times

of flood, as occurs in the Murray (Shiel 1979).

Other species become established during algal

blooms in lakes and rivers, using algal

filaments or mats as substrates for attachment,

and are thus seasonal or facultative plankters.

New taxa only are figured, wilh the excep-

tion of Brachionus lyratus Shephard (Fig. 1),

This species was previously considered to be

synonymous with &. cawdatuy (Ahlstrom

1943), however present samples indicate that

the species is valid.

Abbreviations for the locations of type

material are: ZMK, Zoological Museum, Uni-

versity of Kiel, D-2300, F.R.G,; SAM, South

Australian Museum,

Systematics

ORDER BDELLomaA

(See Shiel & Koste 1979, for known Australian

bdelloid rotifers),

ORDER PLoImMipak Hudson & Gosse, 1886

Family Epiphanidae Bartos, 1959

Liliferetracha subtilis (Rodewald), 1940

Loc: B, Thornton, Vie., A; 17-8, 7.1. 8.9, 28.

Rhinoglena frontaliy (Ehrenberg), 1853

Loe; B, Yarrawanga, Vie, Sp; 14,5 8.2. 12.5,

18, 74

Family Brachionidne Kutikova, 1970

Brachionns quadridentatus {. brevispinus

(Ehrenberg) 1832

Log; L, Boort, Vic. Su; 23.5, 7.9, 6.0, 87,

750,

W. KOSTE & R. J. SHIEL

B. quadridentaius 1. cluniortheularis

(Skorikow) 1894

Loc; B, Wodonga, Vic., Su,

B. vartabilis (Hempel) 1896

Loe: B, Wodonga, Vic., Su

B, lyratus Shephard, 1911 (Fig.1)

Trophi preparation, Rot, No. 023, ZMK,

In Koste (1979) a Brachionuy resembling

that deseribed by Shephard (1911) was

figured. Harring (1913) suggested synonymy

of the form with B, anegularis candatus Bar-

Trois & Daday 1894, Voigt (1937) considered

the form insufficiently known, and Afistrom

(1940) considered it synonymous with B. ar-

guleris. Examination of recent collections sup-

ports Shephard’s comments on the peculiar

Morphological characteristics of this distinctive

species. In particular, the presence of sub-

median spines, absent in B. angufaris, and the

“two knobbed projections (posteromedian

spines) which curve outward in a manner

sugeesting the form of a lyre’, Such foot-

opening spines are not described for 8B. angu-

laris or B, caudatus. On the basis of these

laxonomic characteristics the independence of

B. lyratus in the Formenkreis angularis is

recognized, This now comprises the species

groups angularis, charint, dichatomus, dola-

Aratus, forficula and Iratus (see Koste 1978),

Measurements: Loriea length 120-145 um,

lorica width 90-96 pm, foot-opening width

20-24 pm, head-opening width 60-64 jm.

subitaneous egy 65/45 jum.

2(¢)

Figs |-2 |—Frucliouus lvratus Shephard,

191). ah. Loricu, ventral Fig. 2—A&. bidentate

tL testudlinarius (Jakubskit 1912. 9, Lorica,

dormal, 6, Lonea, ventral, c. Lorea lateral.

Lorica Jength 220 am, (ef. Fig. da, b)-

NEW ROTIFERA FROM AUSTRALIA 135

oc: B, Thornton, Vic., A; 17.8, 7.1, 8.9, 28,

B. dimidiatus (Bryce) 193)

B, Wadonga, Vic., A.

B, urceelarisy sessilis (Varga) 1951

Loc: B, Jabiluka, N-T., W: 25,0, 6.15, 3.7, -.

48,

B, dichotomus reduetus Koste & Shiel, 1979

Loc: B, Eskdale, Vic., Su; 29.2, 7.5, 8.0, 6,

85.

RB. hidentata Anderson, 1889 (Figs 2+)

Loe!

B. bidentata minor 0.ssp.

(FIG. 3a-h)

Material: (6 contracled females, sample No. 295,

in formalin.

Holotype: loricate female, sample No. 295, coll.

28.01.77, R. J. Shiel, Rot. No. 025, ZMK,

Paratypes: SAM, V,2092, Koste collection, Qua-

kenbrtick. F.RAG,

Icanatype: Pig, tlostra 3a,b.

Type Jocality: River Murray, Mannum, §.A.

(34°50'S/ 139° 18'E),

Description: Small barrel-shaped lorica with

six dorsal anterior spines. Short, unforked

marginal spines (cf. Fig. 2c). Basal plate pre-

sent. Semicircular dorsal lorica border. An-

terior border of ventral plate slightly indented

medially. Highly placed circular foot-opening.

Posteromedian spines terminally —button-

shaped. Posterolateral spines absent. In larger

specimens slight facettation dorsally (Fig. 3d,

h). Lateral antennae marginally placed,

Measurements: Lorica length 120-156 pm,

lorica height 52-80 pm, greatest Jorica width

84-108 pm, range of marginal spines 72-104

Discussion; The lorica shows comparative

similarity to that of B, bidenrata ft. inermis

(Rousselet) 1906, The latter however has long

murginal spines, absent in minor. Moreover,

this morph is an intermediate to 8. bidentata

f. testudinarius (Jakubski) 1912 (Fig. 2a—c),

which has a short curved posterior spine, In

the new subspecies the posterior border of the

lorica is specifically semicircular. Comparison

with B. bidentata {. jlrove? (Bartos), 1947.

Syn: B. furenlatuy var, jirevci Bartos, 1947

(Hauer 1963; Kutikova 1970) shows that this

intrasubspecies taxon, in contrast to B. biden-

tata miner, bas forked marginal spines, and

also nceasionally posterolateral spines.

3a) 3(b) ~3(c)

rat Ps9 XY . ™.

oO (f

Ning 3a) Sf pp

is. My 50 ym ‘ 4

3(h) 4,0,

uty [

‘iat

a 4 )

wl vy}

-. eS \. ,

Lie" uc air

Figs 3-5. 3—Braciiionus bidentata minor .s5P.

a. Lorica, dorsal. b,c. Loricu, ventral, d.

Anorher lorica, dorsal, e-@. Dillerent loricas,

ventral. f. Lorica with dorsal structure (all From

the same population). Fig. 4—B. bidentata f.

evindinerius. Lorica, dorsal. Length 1704m,

width 140um. Fig, 5—A_ pliecatilis calongula-

ciensis. ssp, Lorica, dorsal, Lorica length 400

um.

Considering the great variability of the

species B. bidentata an exact taxonomic classi-

fication of the different morphs is difficult. For

example, with regard to length of lorica spine

development, Pourriot (1974) showed experi-

mentally that this depended on the presence of

the predator Ayplanchna brightwelli.

The new subspecies is considered here as a

“dwarf-form" sensu Green's (1977) study,

where food-storage, salinity of biotope, etc.,

caused a reduction of lomea-size in crater

luke rotifers.

Therefore the classification of B. hidentata

minor as a subspecies ie. a genetically dis-

tinct farm, is provisionally documented here,

noting However that only a single collection

is involved.

Loc: R. Mannum, S.A,, Su; 17.0, 8.2, 9.7,

86, 1,020.

Brachionus bidentata f.

(FIG, 4)

In one sample from Lake Nillahcootie, Vic.

(36°53'S/146°01'E) on 2741.78 an individual

animal resembling the f. restudinarius was

collected. Forked marginal spines are absent,

? testudinarius

136

however, and the dorsal lorica is unstructured.

The lorica has a resemblance to Brachionus

quadridentatus var. ancylognathus (Schmarda

1859), but the elongated marginal spines, dis-

tinct lorica basal plate and the tube-like foot

orifice indicate that this is a morph of B.

bidentata.

Measurements: Lorica length 164 um, greatest

lorica width 140 ym, marginal spine length

68 ym, posterior spine length 100 pm.

Loc: L, Nillahcootie, Vic., Su; 26.0, 7.9,

11.3, 24, 55.

Brachionus plicatilis colongulaciensis n.ssp.

(FIG. 5)

Type material: 122 females of different ages, in

formalin, sample number 647, collected by W, D.

Williams, Lake Colongulac, Vic. (May 1979).

Holotype: Loricate female, coll. Williams 23.v.79,

Rot.No.024, ZMK.

Paratype: SAM, V.2093; Koste collection, Quak-

enbriick, F.R.G.

Type locality: Lake Colongulac (salinity 10.4%),

W. Victoria (38°10°S/143°10'EB).

Description: Greatly elongated transparent

lorica. Surface unstructured. Anterior spines

much reduced. Anterior border of ventral

lorica with four short, flat, tongue-like projec-

tions. Posterior lorica margin tapered and

rounded. Foot-opening terminal, lowered

ventrally. Dorsal lateral antennae approxi-

mately level with mid-lorica. Ratio lorica

length: width approximately 2:1,

Measurements: Lorica length (adult 2) 400—

440 um, lorica width 210-240 ym, foot-open-

ing width 40 ym, anterolateral spine develop-

ment —75 ym, subitaneous egg 132-150 X 90-

110 pm.

Discussion; In the population examined, all

adult females had an extraordinary large

lorica, corresponding in appearance to that of

B. plicatilis f. decemcornis Fadeev, 1925. The

latter has a different foot-opening (see Koste

1978) and is smaller. Hauer (1925) describes

an elongated form from Bad Oldesloe with a

cross-sectioned lorica length of only 260 pm.

A lorica of approximately corresponding out-

lines was figured by Ahlstrom (1940) with a

length of 275 ym and a greatest width of 210

pm. Neither of these is in accord with the

Australian find. The greatest lorica length

known to date is 315 ,m,

It is apparent that the new ssp. population

has arisen in Lake Colongulac in response to

specific ecological pecularities of the habitat.

W. KOSTE & R. J. SHIEL

For the anatomy of this Brachionus, see

Koste (1980a). For distribution of the species

group see De Ridder (1960).

Loc: L, Colongulac. Vic., A; 12.7, 8.2, -,

42, 10.4 gm 1-4

Keratella procurva (Thorpe) 1891

(FIG. 6a—k)

This pantropical species, known previously

only in its typical form (see Ahlstrom 1943,

Berzins 1955 and Koste 1978), shows con-

siderable variability in posterior spine develop-

ment and overall lorica size. Paggi (1973)

figures and reports on a series of different

lorica forms (Fig. 6h) from the Parana River,

Argentina.

In the many Australian samples examined,

this species occurred also with variable lorica

forms. The most abundant forms are figured

(6a,f,g,i). A previously unknown form of the

species group (Fig. 6b-e,j,k), notable in

respect to its smallness and form of posterior

spines, is documented below.

Keratella procurva robusta n.ssp.

(FIG. 6k)

Holotype: Female, coll. R. J. Shiel, Keepit Dam.

N.S.W., 24.v.78, Rot. No, 026, ZMK,

Description: Short, squat, relatively wide and

opaque lorica, ornamented with large pustules.

Facetted as in f. typ., although with minor

differences in populations from widely

separated localities. All lorica spines, particu-

larly short posterior spines, with wide bases

(cf. Figs. 6b,j with 6d,h,i). Latter curved

backwards in lateral view. Forms without

caudal spines or with only a single postero-

lateral spine rudiment as in K. tropica (Apstein

1907) not recorded for K. procurva. Compara-

tive morphological characteristics and measure-

ments of known forms of K. procurva are as

follows. In common forms (Figs 11la,f) the

lorica surface is smooth or weakly granulated.

Total lorica length from 155-220 ,m; lorica

width 67-80 pm; anterior spines 19-20, 17-

22 and 30-40 um and posterior spines 22-24

pm (left) and 27-64 pm (right). K. procurva

robusta has a strongly studded lorica surface,

total length 148-150 ym; lorica width 82-90

pm; anterior spines 15-17, 10-15 and 22-23

um; posterior spines 14-15 ,.m (left) and 20-

23 um (right).

Loc: L,B,R, Darling catchment, Su; 10.5—

25.0, 7.4-8.7, 6.4-10.8, 270-1000, 15-1000,

15-115,

NEW ROTIFERA

6(b) 8(c) 6(d)

Fig. 6a. 1891.

(Thorpe)

Lorica, dorsal. Morph wilh dorsolaterally curv-

ing posterior spines. S. Australia. Lorica length

220 nm. b. K. procurva robusta mssp. Lorica,

Keratella procurve

dorsal, length 1S0em. c. Lorica, lateral. d.

Another specimen. e. Subitaneous egg of A. pro-

curva robusta. T-g. K. procurva type, common

form from Australian waters. h. A. procurva,

variations from Argentinian waters, 8S. America

(afer Paggi, 1973). i. K. precurva from

Australian warm waters, N.T. Lorica length to

230 um. j,k. Two forms af K, pracurva robusta

from Darling River waters.

Notholea squamula (Muller), 1786

Loc: R, Donald, Vic., Ay 11.0, 8.0, 11.2, -— =

Anuraeopsis navicula Rousselet, 1910

Loc: B, Yea, Vie. A; 10.5, 7.2, 10.1, 33, -.

A. coelata De Beauchamp, 1932

Loc; B, Jabiluka, N.T,, W; 25.0, 6.2, 3.0, —

Ag.

Family Euchlanidae Bartos, 1959

Euchlanis dilatata *. univetata (Leydig), 1854

Loc: B, Seymour, Vic., W; 10.0, 7.2, 11.6,

2, 330.

E, praxima Myers, 1930

Loc: R. Wyangala, N.S.W., Su; 15.5, 7.3,

10.2, =, =

FROM AUSTRALIA

\37

Dipleuchlanis propatula (Gosse), 1886

Loc: B, Jabiluka, N.T., W; 25.5, 6,2, 2.9, — 62.

Family Mytilinidae Bartos, 1959

Myrilia macracaniha (Gosse), 1886

Loc: B, Jabiluka, N.T., Ws 24.5, 6.3, 5.8, -

59.

M. bisulcata Lucks, 1912

Loc: B, Jabiluka, N.T,, Wi 25.5, 6.2, 2.9, -,

62.

M. crassipes (Lucks), 1912

Loc: B, Jabiluka, N.T., Wz 25.0, 6.2, 3.0, -,

48,

Family Trichotridae Bartos, 1959

Wolga spinifera (Western), 1894

Loc; R, Wentworth, N.S.W,, A; 10.0, 8.0,

10.2, 12, 675,

Family Colurellidae Bartos, 1959

Colurella adriatica Ehrenberg, 1831

Loc: L, Boort, Vic., Su; 27.5, 7.9, 6.0, 67,

750, R. Benalla, Vic., A; 8.5, 7.0, 11.2, 21,

575.

Sguatinella mutica (Ehrenberg), 1832

Loe: B. Yea, Vic.. Ay $9.9, 7.2, 8,5, 0.8 m,

85.

Lepadella ehrenbergi (Perty), 1850

Loc: B, Jabiluka, N.T.. W; 24,0, 6.25, 5.1, -,

42.

L. elliptica Wulfert, 1939

Loc: B, Jabiluka, N-T., W; 25.5, 6.2, 2.9, —

62.

L. rhontboides rhaniboides (Gosse), 1886

Loc: B, Jabiluka, N.T., W; 24.5, 6.3, 5.8, -,

59.

L. rhomboides f curinata (Bonner), 1934

Loc: R, Benalla, Vic., Su; 27.0, 7.6, 7.0, 52,

L. dactyliseta (Stenroos), 1898

Loc: R. Benalla, Vie,. Su; 27.0, 7.6, 7.0, 52,

L. henjamini Harring, 1916

Loc: L. Boort, Vic., Su: 20.0, 7.4, 8.8, — =

B, Jabiluka, N.T., W; 24.0, 6.25, 5.1, -, 42.

L. heterodactyla Fadeew, 1925

Loe: L, Boort, Vic., Su; 20.0, 7.4, 8.8, — —

L. apsicora Myers, (934

Loc; L, Boort, Vic., Su; 23.5, 7.9, 6.0, 67, 750.

L, nehoissi Berzins, 1960

Loc: R, Kinglake West, Vic., Sp.

L, ptilota Berzins, 1960

Loe: R, Clunes, Vic., W.

138 W. KOSTE & R, J. SHIEL

50pm

Fig ?

) 50 ym

Fig 8

8(c) ad

Figs 7-8. 7—Lepadella chenvoluthi nsp- a.

Lorica, yentral, 6. Distal foousegment with

toes enlarged. c. Lorica cross-section. d. Neck

aperture, dorsal. ¢. Ventral aspect, Fig, 8—L,

williaiisi 1.sp. ab, Ventral uspecls of two

loricas. ¢, Lateral view. d. Lorica cross-section.

L. angusta Berzins, 1960

Loe: R, Morang, Vic, Su,

L, marnedactyla Berzins, 1960

Loc} B, Jabiluka, N-T.. We 25.5. 615, 2.9, -

62.

L, rererostyla (Murray), 1913

Loe: L, Boort, Vic., Su; 23.5, 7.9, 6.0, 67, 750,

L.. latusinus (Hilgendort), 1899

Loc; R Benalla, Vic), Su: 27.0, 7.6, 7,0, =, -

Lepadella chengalathj sp.nov.

(FIG. Ta-e)

Type ninterial: 3 lavieate 23, sample number 307,

Holautype: Pemile, sample number 307, call. Ref.

Shicl, Rot No, 021, ZMK.

Uvpe locality: Lake Boort, endorheic (internal)

drainage, near loddon River, Vieloria (36°

US'S/143°45'B),

Deseriptions Rhomboidul lorica (Fig, 7a) with

rounded corners, widest in first third, Mead

opening small, not drawn down ventrally.

Foot-opening semivireular at widest point of

cuudal boundary of dorsal lorica, which is

weakly arched towards interior, Three flexible

foot-urticulations, distalmost slender and

elongated. Toes symmetrical, long, needle-like

and straight (Fig. 7b). Lorica vross-section

shows highly vaulted dorsal lorica with slender

downward-drawn lateral wings. Ventral plate

with delicate double convex keel (Fig. 7e).

Measurements; Total length 135-140 jum,

lorica height 48 jum, lorica length 96 ,m,

lorica width 92 ym, head-opening width 28

wim, foot-opening 28 % 28 um, distal foot-

articulation 19-20 pm, toe-length 33-36 pm.

Discussion; The new species has similarities

With Lepadella benjamini Haring, 1916. In this

species, however, the head-opening is cap-like,

more or less Ventrally drawn down, and the

distal foot-articulation is not elongated (12-

13 pm). CYL. also an Amazonian form described

by Koste (1972, 1978) L, benjamini f. brasi-

liensiv with rounded side rims. The genus is

reviewed by Chengalath (1976).

Etymology; Named after Rama Chengalath,

National Museum of Canada, Ortttiwa, in

uppreciation of years of scientific cooperation

and friendship with W.K.

Loc: L, Boort, Vic,, Su; 23.5, 7.9, 6,0, 67,

420,

Lepadella williamsi n.sp,

(FIG. Sa-d)

Holotype; Locicate female, sample namber 657,

coll, R, J, Shiel, 13.vi,79, Rot. No. 19, ZMK,

Paratype, SAM V,2904; number 657 Koste col-

lection, Quakenbriek, D-4570 FRG.

Type lovality: Ja-Ja Billabong, Jabiluka, N,T,

(12°40'S/133°00'R).

Peseriptions Smoothly oval, highly-vaulted

loriva (Pig. 8d) With ventrally-direeted head-

opening, Dorsal loricu tapers caudally to a

variuble-length dorsal and laterally curved point

(Figs 8a,b), Foot-opening narrow and ends

at base of dorsal lorica projection. Only three

flexible, approximately equal length foot sex.

ments visible. Last segment with long, dorso-

laterally curved sharp toes.

Measurements, Total lorica length 112-116

pm, lorica height —56 »,m, lorica width 60-64

pm, toe length 36-40 am, foot-opening 17-20

* 19-20 am, head-opening 33-36 * 28-30

win, distal foot-segment length 10 jm, caudal

lorica projections 19-28 jum.

Diveussion: The new species resembles the

Species group L, acuminata, Which also occurs

in Australia (Figs 9,10), and which is charac-

icrised by a more or less clongated and ovea-

sionally split lorica point, However the margin

of the foot-opening of this projection is closed

(Fig. Yb, 10b). The lateral antennae, which are

NEW ROTIFERA FROM AUSTRALIA

dorsal to the basis of the caudal projection, in

contrast to L. williamsi are very narrowly

placed. In L. acuminata and its various modi-

fications (Koste 1978) the dorsal margin of the

head-opening is more or less concavely cut out.

The new species was previously seen in a

sample from a tank near Kuala Lumpur,

Malaysia collected by C. H. Fernando, Uni-

versity of Waterloo, Ontario, Canada.

Emmolagy: Named after W. D, Williams, Dept

of Zoology, University of Adelaide for assis-

tance in collecting rotifer material and support

toward this work.

Loc: B, Jabiluka, N.T., W; 25.5, 6.15, 2.9.

5, 62.

Heteroleapdella ehrenbergi (Perty), 1950

Loe: B, Eskdale, Vic. Su; 29.2, 7.5, 8.0, 6,

85,

Family Lecanidae

Lecane hernemanni (Ehrenberg), 1834

Loc: B, Yea, Vic., A; 19.9, 7.2, 8.5, .8 m, 85.

B, Jabiluka N.T., W, 24.5, 6.3, 5.8, — 59.

L. ludwigi (Eckstein), 1893

B, Jabiluka, N.T., W; 25.5, 6.15, 2.9,

L. aculeata (Jakubski), 1912

B, Jabiluka, N.T.. W; 24.0, 6.25, 5.1,

L. stichdea Harring 1913

Loe: R. Mannum, S.A. W: 11.0, 8.4, 10.8,

40, 575.

L. curvicornixy (Murray), 1813

Loe: B, Jabiluka, N.T.. W; 25.0, 6.2,

48,

L, furcéta (Murray), 1913

Loe: B. Jabiluka, N.T., W: 24.5, 6.3, 5.8, -,

59.

L. grandis (Murray), 1913

Loc: B, Jabiluka, N.T., W; 25.0, 6.2, 3.0, -,

48.

L. doryysa Harring, 1914

Loc: B, Jabiluka, N-T., W; 24.5. 6.3, 5.8, -

59,

L. crepida Harring, 1914

Loc: B, Jabiluka, N.T., W; 25.0, 6.2, 3.0, -

48.

L, tenuiseta Harnng, 1914

Loc: B. Jabiluka, N.T,, W; 25.0, 5.85, 2.2,

-, 29,

L. lunaris crenata (Harring), 1923

Loc: L, Yarrawonga, Vic,, Su; 24.2, 7.7, 8.6,

—, 60.

9 (a)

50 ym

I (a) l(b) tI {c)

Figs 9-Il. 9—Lepadella acuminata (Ehren-

berg), 1834 from N.T. a. Lorica, dorsal,

b. Foot-opening and toes, ventral, Fig. 1O—L.

wcwninata form with abbreviated caudal loricu

point from N_T., Australia, a, Dorsal. b, Foot-

opening and toes, ventral. Fig. 11—Lecane

(Monostyla) hamata Vietariensis nassp. a. Ven-

tral view, lorica contracted, b. L. hamata

hamata Stokes: 1896, ¢, L. sinueata Hauer, 1938.

L. unguitata (Fadeew), 1925

Loc: B, Jabiluka, N.T.. W; 25.0, 6.2, 3,0, -

48,

L. acronycha Harring & Myers, 1926

Loc: B, Jabiluka, N.T.. W: 25.0, 6.2, 3.0, —,

48.

L. inopinata (Harring & Meyers), 1926

Loc: L, Wyangala, N.S.W., Su; 27.0, 7.4, 7.5,

, 245,

L. pertica Harring & Myers, 1926

Loc: B, Jabiluka, N.T., W; 24.5, 6.3, 5.8. -,

L, elsa Hauer, 1931

Loc: B, Alexandra Vic., Sp; 20.0, 7.2, 9.1, —

L, nodosa Hauer, 1938

Toc: B, Jabiluka, N.T., W: 24.5, 6.3, 5.8. -,

L. ruttneri Hauer, 1938

: L. Boort, Vic., Su; 20.0, 7.4, 8.8.

L. hamata victoriensis n.ssp,

(FIG, 11a)

Type material: 2 loricute 99. sample number 263,

Holotype: loricate 2, sample number 263, coll. R.

J. Shiel (14.x.77) Rot. No. 029, ZMK,

140

Type locality: Billabong “Goulburn View”,

near Alexandra, Victoria (37°13’S/145°42’E)

from Juncus bed, 30 cm depth.

Description: Both anterior points of dorsal

lorica at head aperature are congruent with

ventral lorica, therefore not visible. Whereas

this aperature in type flat or deeply curved,

in spp. it is a deep trapezoid notch, basally

8 um wide, bordered by light, curved lines.

Lorica outline widely oval. Ventral plate

smaller than dorsal plate. Toe gradually taper-

ing from point of insertion at second foot

segment.

Discussion: Morphologically, this ssp. shows

several characteristics in agreement with L.

(M.) sinuata Hauer, 1938 (Fig. 11c). A simi-

lar rotifer also was described from India by

Wulfert (1966) as L. arcuata (Bryce), how-

ever the notch between the anterior spines in

this latter form are otherwise shaped, and sig-

nificant differences are seen in the measure-

ments.

Measurements (in pm) are given in the

following sequence: overall length, dorsal plate.

ventral plate anterior transverse width, toe

length, form of neck opening for each form of

L. hamata, f. typica 103-136, 61-88 xX 52-

66, 77-98 X 40-60, 18-30, 26-38 double

semicircular. v. sinuata 108-110, 74-76 X53-—

55, 80-82 X 41-46, 21, 28, curved. v. arcuata

100, 52 X 56, 70 X 40, 25, 28, semicircular.

v. thienemanni 113-123, 64-70 X 62-64,

77-88 X 46-55, 26-35, 33-34, ventral flat-

concave, dorsal straight. victoriensis 124, 84

xX 64,92 X 56, 24, 32. trapezoid. Fig. 11a

shows morphological differences of the new

spp. from that described by Stokes, 1896 (Fig.

11b). In contrast to L. h. victoriensis, L. h. var.

thienemanni has a characteristic horizontal

dorsal lorica margin, and the toe is distended

in the middle.

Loc: B, Alexandra, Vic., Sp; 20.0, 7.2, 9.1,

2, 115.

Family Proalidae Bartos, 1959

Proales fallaciosa Wulfert, 1937

: B, Jabiluka, N.T., W; 24.5, 6.3, 5.8, -,

Family Lindiidae Dujardin, 1841

Lindia torulosa Dujardin 1841

: B, Yea, Vic., W; 11.0, 7.2, 6.1, 17, 170.

L. deridderi Koste, 1979

: B, Wodonga, Vic., W; 10.2, 7.2, 9.0, 4,

W. KOSTE & R. J. SHIEL

Family Notommatidae Remane, 1933

Itura myersi Wulfert, 1935

Loc: B. Wodonga, Vic., Sp; 14.7, 7.1, 4.1, 5,

240.

Eothinia elongata (Ehrenberg), 1832

Loc: B, Wodonga, Vic., Sp; 14.7, 7.1, 4.1,

5, 240.

Monommata grandis Tessin, 1890

Loc: B Jabiluka N.T., W; 24.5, 6.3, 5.8. -,

59,

M. actices Myers, 1930

Loc: B, Jabiluka, N.T., W; 25.0, 6.15, 3.7, -,

48.

M. arndti Remane, 1933

Loc: B, Alexandra, Sp; 20.0, 7.2, 9.1, -, -.

Notommata glyphura Wulfert, 1935

Loc: B, Alexandra, Vic., A; 17.8, 7.2, 8.9, 8,

Cephalodella eva (Gosse), 1886

Loc: B. Eildon, Vic., A; 17.9, 7.2, 9.2, 0.5,

87.

C. mucronata Myers, 1924

Loc: R, Mungindi, N.S.W., A; 16.0, 8.1, 9.2,

C. panarista Myers, 1924

Loc: B, Jabiluka, N.T., W; 25.5, 6.2, 2.9, -,

62.

C. ventripes Dixon-Nuttall, 1901

Loc: B, Wodonga, Vic., Sp; 14.7, 7.1, 4.1, 5,

240.

Family Trichocercidae Remane, 1933

Trichocerca cavia (Gosse), 1889

Loc: B, Eildon, Vic., A; 18.0, 7.1, 11.0, 0.5,

70.

T. collaris (Rousselet), 1896

Loc: B, Jabiluka, N.T., W; 24.5, 6.3, 5.8. -,

59.

T. chattoni (De Beauchamp), 1907

Loc: L, Wyangala, N.S.W., Su; 27.0, 7.4, 7.5,

0.5, 245.

T. myersi (Hauer), 1931

Loc: B, Jabiluka, N.T., W; 24.0, 6.25, 5.1,

—, 42.

T. flagellata Hauer, 1937

Loc: B. Jabiluka, N.T., W; 18.0, 6.1, 6.7, —, 63.

T. mus Hauer, 1938

Loc; L, Nagambie, Vic., Su; 15.0, 7.4, 8.9,

1.3m, -.

T. jenningsi Voigt. 1957

Loc: B, Jabiluka, N.T., A; 29.0, 6.5, 2.9, —

28.

NEW ROTIFERA FROM AUSTRALIA 141

T. similis erandis (Hauer), 1965

Loc! B, Wodonga, Viec.. Sp; 15.5, 7.0. 10,8.

16, 43,

YT. agnatha Wulfert, 1939

Loc: R, Echuea, Vic., Su; 15.0, 7.6, 9,0, — ~.

Ascomorpheila valvovicola (Plate), 1886

Loc: B, Thornton, Vie. A; 12.4, 7.1, 8.6, 2,5.

11S.

Family Gastropodidac Remane. 1933

Ascoimorphe saltany Bartsch, 1870

Loc: L. Burtinjuck, N.S.W,, Su; 26,0, 7.6, 8.0,

1, 190,

Family Synchaetidae Remane, 1933

Synchaeta tavina tavina Hood, 1893

Loc: L, Kerang, Vie. W.

3. litoralis Rousselet, 1902

Loc! B, Wodonga. Vic., W; 10.2, 7.2, 9.0, 4

154,

Family Dicranophoridue Remane, 1933

Dicranepherus uncinatus (Milne), 1886

Loc: B, Wodonga, Vie, A,

D, aquilus (Gosse), 1887

Loc: R, Mungindi, N.S.W., Ai 16,0, 8.1, 9.2,

Dicranophorus claviger australiensis n.ssp.

(FIG. 12a.b)

Type material; 14 92, sample number 669,

Hototype: female, coll. 13.vi.79, R. J. Shiel, Rot.

No. 027, ZMK.

Type locality: Ja Ja Billabong, Magela Creek

floodplain, confluent of Alligator River near

Jabiluka, N.T. (12°40'8/132°50"))

Description: Elongate spindle-shaped body.

Integument rigid, longitudinal lines from neck

to short horizontal line on dorsal part, Head

purt cylindrical with moderate concave out-

lines. Small prolongation of dorsal lorica over

foot. Toes extremely Jong and slender, curve

somewhat outward, end in acute pointed claws

seen Only in lateral view. Corona with two

frontal eyes and paired knobbed palps, Trophi

large. Rami terminate wilh smal) tecth as in

the trophi of D. caudatus (Fig, 12c) but have

broad lamellar alula, which are apically clon-

gated, ending in pai of double short teeth.

Unci each have only a tooth. Short fulerum

has broad triangular form. Manubria shghtly

curved, spatulate ended, Beneath unci contact

point is lamellar triangular clement. Preserva-

tion Ww formalin precludes discussion of internal

organization.

Discussion: This species is related to D. cau-

datuy, from Victoria, and D. claviger, from

South America by virtue of ils morphology,

Comparative information on the related forms

is given below. Affinity of this ssp. with D.

claviger (Hauer) 1965 is suggested by the

palp number and similar trophi structure,

although D. claviger (= Itura claviger Hauer,

1965) has a different shaped fulcrum, shorter

toes and a significantly shorter overall length,

Measurement (in pm) and comments are

given in the sequence overall length, greatest

width, palp number, palp length, toe length,

trophi length, manubrium form, uncus, ful-

crum, rami, manubrium, teeth on ramus point.

supra-rami teeth, supra-rami teeth length, dis-

tribution: D, caudatusy Ehrenberg, 180-310,

90, 1, 9-10, 69-77, 34-36, sticklike, 13. 6,

21, 25, — absent, —, cosmopolitan; D. caudatus

braziliensis Koste, 1972, -330. — 2, 2, 84-88,

48. terminally crutch-like, 32, 8, 26, 32, 4.

absent, — Amazon. S. America; 2. claviger

(Hauer) 274, 100. 2, 16, 24-44, 41-46, ter-

minally broad, 17, ti, 32, 24, 4-5, oralplate

(2), =, Amazon, S. America; 0 claviger i.ssp.,

—532, -120, 2, -21, 155-164, 50-53, termin-

ally broad, 34, 13. 40, 39, 6, present, 18, N,

Aust.

Loc: B, Jabiluka, N.T., W; 23.5. 3.8, 2.4,

=, 30.

Aspelta pitta Harring & Myers, 1928

Loc: B, Wodouga, Vic,, W; 10.2, 7.2, 9.0,

4, 154,

Encentrum gibbosum Wulfert, 1936

Loc: R, Wangaratta, Vie, A; 12,0. 7.7, 10.0,

ORDER Gwesiotrocia De Beauchamp, 1965

Family Testudinellidae

Testudinella parva (Ternetz), 1892

Loc; B, Jabiluka, N.T.. W; 250, 6.2, 3.0,

-, 48.

T. emarginula (Stenroos), 1898

Loc: B, Yea, Vic., A; 12.0, 7.3, 9.8, —-.

R. Benalla, Vic., Su: 27.0, 7.6, 7.0, -, —

T. tridentata Smirnov, 1931

Loe: L, Yarrawonga, Su, 24.2.. 7.7, 8.2, 22,

160.

B, Jabiluka, N.T., W: 24.5, 6.3, 5.8. -, 59.

T. amphora Hauer, 1938

Loc: B, Jahiluka, N-T., Wy 24.5, 6.3, 5.8, -,

59,

142 W, KOSTE & R. J, SHTEL

Fig. 12, Dicranophorus claviger anstraliensis ssp.

a. Dorsal view, total length 532 4m. b. Trophi,

dorsal view, length 53 um, c. Comparative view

of trophi of DB. caydums (Ehrenberg, 1834),

length 35 um,

Testudinella walkeri n.sp.

(FIG. 13a,b,c,d,e)

Type material: 6 9°, preserved in formalin, sample

number 659.

Holotype; Lovicale female, sample number 659,

coll. 13.vi.79, R. J. Shiel, Rot. No. 020, ZMK.

Type locality; Mine Valley billabong, Mageia

Creek floodplain, tributary of Alligator River

near Jabiluka. N.T. (12°40'S/132°50°E).

Description: Juyenile lorica (Fig. 13b,e) widely

oval, strongly circular outline in adults (Fig.

13a). Dorsal lorica slightly concave at widest

point. Ventral Jorica under neck-aperature with

keel-like folding, two edges of which curve

outwards to lower lorica rim. Foot-opening

slit-like under middle of ventral lorica, Dorsal

anterior rim of head-aperature with rounded,

bulge, medially lightly notched (Fig. 13b). In

poor preparations this can appear concave

(Fig. 13¢c). Lorca end with shallow indenta-

tion, Lateral antennae located slightly above

lorica midline. Lorica cross-section shallow,

triangular (Fig. 13d).

Measurements; Lorica length overall 100-112

pm. greatest lorica width 75-98 pm, neck

aperature width 40-44 ym, greatest Jorica

height in midlme 20-25 ym, foot-opening 20

pM Over the posterior Jorica rim, foot-opening

width 20-24 jm.

Discussion: The new species belongs on the

Formenkreis ineisa (see Koste 1978), A

typical form from this group from the same

sample is shown in Fig. 14, All are described

with oval or egg-shaped lorica outlines, as are

the adult individuals of the brycei-amphora

group (Koste 1978). With the exception of T’,

amphora Hauer, 1937, neither of these groups

has the ear-shaped lateral elevation of the

dorsolateral rim of the neck aperture.

The new species is characterised by this

projection on the upper rim of the wide lorica,

by the presence of the two prominent ventral

divergiiig lines which begin at the keel-like

crease under the ventral margin of the neck

aperture,

15(b) Se

15 (a)

Figs 13-15. 13--Yestudinella walker? nsp. a.

Ventral. b, Anterior lonca detail, contracted,

c Juvenile Jorica, ventral. d. Lorica cross.

section, e¢. Species from Malaysia, lorica,

ventral, Single individual collected, Fig, 14—T.

incisa Yar. emarginula (Stenroos), 1898, Lorica

length 110 2m, lorica width 85 em, Fig. 15—

TW ainphora Hauer, 1937 from N.T. a. Dorsal

b. Ventral, oblique. Lorica length 96 am, Joricu

width 78 wm,

NEW ROTIPERA FROM AUSTRALIA 143

A lorica of similar form but lacking the

wide ventral keel was. found in a sample trom

Malaysia (coll, C. H. Fernando, University of

Waterloo, Canada),

Comparative measurements (in pm) are

given in the sequence lorica length, lorica

width. fout-opening, neck aperture, lorica

cross-section: T. walkeri nsp, 100-112, -98,.

slitlike, With lateral “ears” 40-44, shallow trian-

gular, 7. sp. fram Malaysia, 136, 84, angular

16 ™ 10, with “ears” 64, shallow triangular;

T. amplhera, 90-95, 60-78, slittike 18-20,

with “ears”, triangular, T. bryce’, 85, 58, slit-

like, medially tongued-shaped, triangular; T,

incisa ve emarginula, 80-130, 65-82, stitlike,

medially shallow, tongue-shaped shallow tri-

angular,

Loe: B, Jabiluka, N-T., Wy 24.5, 6.3, 5,8,

=~, 59,

Erymalogy: Named after Dr K, BF, Walker,

Department of Zoology, University of Ade-

laide, in appreciation of support during a Ph.D,

program by RIJS,

Pymily Flosculariidae Harring, 1913

Piygura furcillate (Kellicolt), L889

Loc: L, Boort, Vic., So, 23.5, 7.9, 6.0. 47,

750.

Po meliceria vy mucicola (Kellicott), 1889

Loe: B, Wadonga, Vic., Su.

P. tacita Edmondson, 1940

Loc: Bo Yea, Vic., Az 19.9, 7.2. 8&5, 8 m. 35,

Family Hexarthridae Bartos, 1959

Hexurthra polyodonta (Hauer), 1957

Loc: B, Seymour, Vic., Sp: 18.0, 7,2, 9.4, —

265.

Family Filiniidae Barts, 1959

Filinia holimarini Koste, 1980

Loe: R, Manoum, S.A., Su A; —28,0, 7.7-8.4,

-10,.8, —]35, =1080,

F australiensiy Koste, 1980

Loc: R. Mannum, S.A., Su; 17.0, 8.2, 9.7. 88,

1020.

Acknowledgments

The following are thanked for making collec-

tions or intormation available; Dr B. Berzins

(Sweden); De T. J. Hillman (Wodonga); Ms

I, J. Powling (Melhourne) and Mr R. D. Tait

(fabluka), Pancontinental Mining is thanked

far use of facilities and for hospitality during

fieldwork at Jabiluka, N,T. The material from

which these records were derived was collected

by RIS during a Ph.D. programme at the

University of Adelaide supported by a Com-

monwealth Postgraduate Research Grant. Prof

W. D. Williams und Dr K. F. Walker are

thanked for their support during this project,

Microscopic work by WK was made possible

with the assistance of the Deutschen For-

schungsgemeinschaft, Bad Godesberg, Bonn,

F.RG.

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HETEROMORPH AMMONITES FROM THE ALBIAN OF SOUTH

AUSTRALIA

BY K. J. MCNAMARA

Summary

The heteromorph ammonite Protanisoceras Spath is described from Australia for the first time. Five

forms are recognised from the Albian Oodnadatta Formation in South Australia, including P.

auriculum sp. nov. and P. gracile sp. nov. By comparison with species from the Albian of Europe, a

Middle Albain age is suggested for part of the Oodnadatta Formation in which they occur. In

addition Appurdiceras cordycepoides (Etheridge 1905) is redescribed and the relationships of the

genus reassessed; a species of Hamites is described; and the Late Albian species Anisoceras sweeti

sp. nov. described.

HETEROMORIM AMMONITES FROM THE ALBIAN OF SOUTH AUSTRALIA

by K. J. McNAMARA®

Summary

McNamara, K, J, (1980) Heteromorph ammonites from the Albian of South Australia. Trans.

R. Soc. §. Aust. 104(6), 145-159, 28 November, 1980.

The heteromorph ammonite Pratanisoceras Spath is described from Australia for the first

lime. Five forms are recognised from the Albian Oodnadatta Formation in South Australia,

including P. auriculam sp, nov, and P. gracile sp, nov. By comparison with species from the

Albian of Burope, a Middle Albian age is suggested for part of the Oodnadalta Formation

in Which they occur, In addition Appurdiveras eardycepoides (Etheridge 1905) is redeseribed

and the relationships of the genus reassessed; a species of Hayites is described; and the Late

Albian species Anisoceras sweeti sp. noy. described,

Introduction

Ammonites form a much less important part

of the marine Cretaceous fauna of the Great

Artesian Basin in South Australia than ip

Queensland; hence few species have been de-

scribed, Albian ammonites were first described

from S.A, by Etheridge (1905) who de-

seribed “Haploceray sp,, Atiisaceras. (2?) sp.,

Ancyloceras cordycepoides and Criveeras

flindersi”® {rom the area of Dalhousie Springs.

The “Haploceras” is probably Falciferella (sce

helow). Whitehouse (1926) proposed Appur-

diceras to accommodate A. cordycepoides,

while “C.' flindersi belongs in Myloceras

(Reyment 1964a; McNamara 1978), The only

other Albian ammonites to have been de

scribed from S.A. are Faleiferella breadeni and

F. reymenti Brunnschweiler (1959) and a Late

Albian fauna including species of My/oceras

und Labeceray described by Reyment (1964

a,b). Ludbraok (1966) illustrated specimens

which she referred to Myloceray axongiides

(Etheridge) and Lebeceray papularum While-

house.

The present study is based primarily on col-

lections from the Albian Oodnadatta Forma-

lion housed in the palacontolagical collections

of the S.A, Department of Mines & Energy

(GSSA). The specimens were collected from

caloarcous nodules, which occur within a soft

#ypscous shale. mainly from Algebuckina 17

(Ludbrook 19646), 32 km SSE of Oodnadatta

at lat. 27°499°S, lone. 135°344°E. Additional

specimens are from Toodla 8, which is 3 km

SW of MI Arthur at lat, 27°31'S and long.

145°41'B (Fig. 1).

Specitnens identified from these localities

(OODNADATTA 1.250000 geological map

Sheet) are:

Street,

* Western Australian Museum, Francis

Perth, W.A, 6000.

Protaniseceras auriculum sp. noy.. P,

gracile sp. nay., P. aff. gracile sp. nov.,

Hamites cf. attenuatus J. Sowerby 1814,

Falciferella sp. (Ludbrook 1966, p. 44).

The second collection on which this work

is based was obtained by G. Sweet frora the

Maree Subgroup and presented to the National

Museum of Victoria (NMV) in 1914. The

specimens arc recorded as coming from “Prim-

rose Springs, Peake Station”. Ludbronk (1966)

considered that this locality may be near

Primrose Hill at 28°10'S, 136°25°E. From an

carly description, she now considers that

Primrose Hill and Springs 1s a mound spring

with seepage at the base and that the various

Stratigraphy of the | nore

|| Qodnadatta region carr

| c. z “Mount Senin

Kin Sarelstane Mn

DALHOU SLE a_i 4

SPINES

S'5,_0 ~ 500m

|| >| Woanitnd ge

oO, S| Sone Mer =

| = FORMATION

2 Goatkiana Member

rt ONT

a | Jj)S 2) surtooc

r x

\ a

r= |

200m

SHALE

250m

“CADNA.OWIE "300m

P| “OS ey bt FORMATION

Ovni |

VEE CRIN AG «

BY wo

r ' ar Fe

WUMROSL

SURINGS

— «= ailyiy

ah Brwal Paw ality

Fig. |. Map showing fossil localities mentioned in

text. Aptian/Albian boundary after Ludbrook

(1966, Map 2). Stratigraphic information after

Freylag (1966, Fig. 1).

146 kK. J.

specimens collected from *Primrose Springs’

are frorn the general area along he Neales

in the NE of the WARRINA 1:250 000 map

sheet where both Aptian and Albian strata

occur (Ludbrook 1966. Map 6: Thonwon

1980). Specimens identified from this locality

are:

Ajlisoceras sweeti sp. nov. Prorant-

soceras sp. A, P. sp. B, Hamiter cl,

alfenuaiks J, Sowerby 1814, Sarvmartine-

ceras (Singevia) fontinale (Hudleston

1890),

The age of the rocks at this locality is dis-

cussed below,

Finally, Appurdicerus cordycepoides (Ethe-

ridge 1905) is redeseribed and reinterpreted

an the basis of Etheridge’s syntypes from the

Oodnadatta Formation al Dalhousie Springs

{Fiu, 1). one of which is housed in the S.A.

Muscum (SAM), whilst the other has been

located in the NMY, All material was collected

from surface outcrop,

Systematic palacontology

Family ANISOCERATIDAE Hyate 1900

ANISOCERAS Pictel 1854

Type species: Hamites saussureanty Pictel in

Pictet & Roux 1847,

Anisoceras sweeti sp, nov

FIGS 2, 6D

Eyvitelogys Named aller G. Sweet whe

ohtzined the specimeie

Holetype> NMV_ P52328, an incomplete

phragmocone from “Primrose Springs. Peake

Station”.

Paratypes; NMY P52325, an inconiplete

phragmocone, and NMY P52326, an incam-

plete body chamber; both from same locality

as holotype.

Age; Late Albiaiy.

Diagnasis: Species of Anisoeeras in which

lateral and ventro-lateral ribs may cover up to

three ribs; ribs broad and strongly prorsira-

diate on phragmocone, Lateral Jobe of suture

three mes width of umbilical lobe,

Deseription; Complete shell form unknown;

description based on straight fragments, Whorl

height slightly greater than whorl width, Phrag-

mogone known from whorl height of 20-24

mov Ornament consists of coarse, prosiradiate

ribs which arise from Jateral tubercles in twos

or threes, and form loop with circular to

clongate ventrolateral tubercles. ‘The lewped

McNAMARA

ribs form a swollen bundle between which

usually lics one relatively depressed inter

calated ib between the looped ribs, On dorsum

are 12 ribs in a distanee equal to the wharl

height; ribs well developed on dorsum. Maxi-

mum known height of body chamber 27 mm.

Ornament similar to that on phragmocone,

though tubercles a little more widely spaced.

Ventrolateral tubercles more elongate than

on the phragmocone. Lateral lobe of suture

bifid and large, covering more than bulf flank

of phragmocone; three times width and about

twice height of bifld umbilical lobe,

Discussion: A. sweeti is similar to A. armatum

(J. Sowerby 1817) from the Late Albian

Stolicrkia dixpar Zone (Cooper & Kennedy

1979: Scholz 1979) in possessing prominent

looped ribs with usually one intercalated rib.

However, the ribs are only looped in pairs in

A, armatum. Furthermore the ribs are more

strongly prorsiradiate in A. sweerl. The two

species can most easily be distinguished by the

relative sizes of the lateral and umbilical lobes

of the suture. In 4. armatum they are of

approximately equal size or the lateral is just

slightly larger than the umbilical (Scholz 1979,

Fig. 8), In A. sweeti the lateral Jobe is very

large, being three times the width of the

umbilical lobe

In A. heasi Cooper & Kennedy (1979)

three, or four, cribs may be looped between the

tubercles, Mowever, the nbs are much finer

than in A. sweeti.

APPURDICERAS Whitehouse 1926

Yvpe speciexr Ancyloceras cordycepoides

Etheridge 1905 p, 14, Pl 1, figs 3-5, Pl, 2,

fig. 4; by original designation of Whitehouse

1926, p. 229.

Emended diagnosiv: Coiling ancyloceratid,

Ribs strongly developed, widely spaced; bifur-

cule laterally and at umbilical tubercles on

shaft. Ventrolateral spines regularly developed,

bases covering one to three ribs. and forming

‘loop and button’ ornament across venter-

Ventrolateral spines on different ribs from

umbilical tubercles, Umbilical lobe of suture

bifid.

Remarks: Whitehouse (1926) — proposed

Appurdiceray lo accommodate Aneyvloceras

cordycepoides Etheridge, distinguishing it from

other Australian heteromorphs by its

proninent ventrolateral spines. Whitchouse

Yuestioningly placed a single labeceratid speci

men from Old in thes genus, calling it 4.(?)

ALBIAN HETEROMORPH AMMONITES 147

Fig, 2. Anisoceras sweeti sp. nov.; NMV P52328, holotype, A, lateral view, B, ventral view; C, NMV

P52326, paratype, dorsolateral view; from “Primrose Springs”, Peake Station; Oodnadatta Formation,

Late Albian; all x 1.

etheridgei, with the result that Appurdiceras

itself came to be thought of as a subgenus of

Labeceras (Wright, in Arkell et al. 1957;

Reyment 1964a; Klinger 1976) which bears

ventrolateral tubercles. A.(?) etheridgei is

quite unlike A. cordycepoides, being a true

labeceratid which has ribs which do not bifur-

cate on the flanks of the shaft, as they do in

A. cordycepoides, and which do not form the

characteristic anisoceratid looped ribs across

the venter. The umbilical lobe of labeceratids

is trifid, whereas in Appurdiceras it is bifid.

Consequently, Appurdiceras is herein

regarded as an anisoceratid and not a sub-

genus of Labeceras. Whitehouse (1926)

included Jdiohamites spiniger (J. Sowerby)

from the English Late Albian in Appurdiceras.

He also noted a similarity with Hamites

nodosus J, Sowerby. This latter species was

made the type of Heteroclinus by Casey

(1961). However Klinger (1976) places this

genus in synonymy with Protanisoceras (see

below).

Unlike species of Anisoceras and Protani-

soceras, which may bear both ventrolateral

and lateral tubercles or spines, Appurdiceras

possesses ventrolateral and umbilical tubercles.

It can also be distinguished from these two

genera by the umbilical bifurcation of the ribs

on the shaft at tubercles which do not form

by the coalescence of the ribs bearing the

ventrolateral tubercles or spines, but by the

coalescence of an intercalated rib with one

which does bear a ventrolateral tubercle, The

ribs may also occasionally bifurcate laterally.

Species assigned to /diohamites tend to have

numerous, fine ribs between the tuberculate

ribs (Spath 1939), though as Klinger (1976)

has noted, /diohamites grades into Anisoceras.

Anisoceras and Protanisoceras differ from one

another in the nature of the suture (see

below). Whereas the umbilical lobe is trifid

in Protanisoceras it is bifid in both Appurdi-

ceras and Anisoceras.

Appurdiceras cordycepoides (Etheridge 1905)

FIG. 3

1905 Ancycloceras cordycepoides Etheridge, p.

14, Pl. 1, figs 3-5, Pl. 2, fig. 4.

1909 Crioceras cordycepoides (Etheridge);

Etheridge, pp. 142, 156, 159, 160.

1926 Appurdiceras cordycepoides (Etheridge);

Whitehouse, p. 230.

21964 Labeceras (Appurdiceras) cordycepoides

(Etheridge) Reyment, p. 25, ?PI. 1, figs

6 & 7.

1969 Appurdiceras cordycepoides (Etheridge);

Day, p. 156.

non

1966 Labeceras (Appurdiceras) cordycepoides

(Etheridge); Ludbrook, p. 190.

Lectotype: Herein designated: NMV P30032,

from Dalhousie Springs (DALHOUSIE

1:250000 geological map sheet) figured by

Etheridge (1905, Pl. 2, fig. 4).

Paralectotype: SAM P2990 from Dalhousie

Springs; figured by Etheridge (1905, Pl. 1,

figs 3-5).

Age: Late Albian.

148 K. J, MCNAMARA

Diagnosis: As for genus,

Description: Phragmocone initially ovoid in

cross section and forms an open criocone for

one whorl, then opens into a shaft. Whorl of

lectotype has maximum radius of 22.8 mm. At

a quarter whorl, whorl height is 4.5 mm; at

commencement of shaft it is 8.5 mm. Early

part of whorl damaged, and it is not known

whether ribs are tuberculate. Ribs are known,

however, to be rectiradiate and not bifurcant.

Whorl section of shaft sub-circular. Ornament

changes on shaft such that ribs become more

widely spaced than on coiled, early part of

phragmocone. Early ribs on shaft infrequently

bifurcate on flanks. Bifurcations more common

along shaft toward crozier. At these bifurca-

tions tubercles are not developed. Bifurcations

more commonly occur umbilically between a

rib which bears a ventrolateral spine and an

intercalated non-spinose rib. Ribs more

strongly developed along shaft. Ventrolateral

spines appear as rounded tubercles on internal

mould. Across venter ribs which connect

spines form a raised swollen band. A ‘button

and loop’ ornament is formed across ventor by

coalescence of three ribs at ventrolateral

spines. Initially ribs on shaft rectiradiate, but

become increasingly prorsiradiate adapertually.

On dorsum ribs less well-developed, but do not

disappear. Shaft almost twice length of maxi-

mum diameter of coiled phragmocone, Ada-

perturally the body chamber recurves to form

crozier. Paralectotype reaches a maximum

whorl height of 16 mm and a maximum whorl

width of 14.5 mm. Suture incompletely

known: umbilical lobe bifid and narrow;

internal lobe trifid.

Discussion: Since the original description of

the two type specimens the only specimens

ascribed to this species are two from the Late

Albian of Fossil Creek, Wooldridge Limestone

Member, Oodnadatta Formation, locality

5/550/1, 42 km NW of Oodnadatta (Reyment

1964a) and specimens from Oodnadatta For-

mation, Algebuckina 17 (5/571/17), 13 km

W of Mt Dutton (Ludbrook 1966). However,

it is not possible for me to assign Reyment’s

fragmentary specimens to A. cordycepoides

with any certainty as, although seemingly pos-

sessing an ovoid to subcircular whorl section

and ventrolateral tubercles, there is no indica-

tion of bifurcation on the flanks of the shaft,

In his description of these specimens Reyment

does suggest the presence of occasional bifur-

cations. If these specimens are true members

of A. cordycepoides their occurrence with

species of Myloceras and Labeceras indicates

that Appurdiceras may be a Late Albian form.

Specimens referred to A. cordycepoides by

Ludbrook are species of Protanisoceras (see

below).

Etheridge’s specimens were collected by

H. Y. L. Brown from the region of Dalhousie

Springs. Ludbrook (1966) has recorded both

Albian and Aptian molluscs from this area.

In addition to describing A. cordycepoides

from the Dalhousie area, Etheridge described

and illustrated other ammonites which have a

Late Albian, rather than Aptian, affinity, in-

cluding the Late Albian Myloceras and

Labeceras,

The development of ventrolateral spines is

seen in other anisoceratids, such as Anisoceras

(Klinger 1976), Idiohamites (Spath 1939)

, lectotype, lateral view; SAM

P2990, paralectotype, B, lateral view, C, ventral view; from Dalhousie Springs; Oodnadatta Forma-

tion, Late Albian; all x 1.

ALBIAN HETEROMORPH AMMONITES 149

and Protanisoceras (Spath 1939). The two cordycepoides, differ in lacking the bifurcation

species from the English Late Albian, Idio- of the ribs on the flank of the shaft and having

hamites spiniger and Protanisoceras nodosum, lateral tubercles developed on the same ribs as

with which Whitehouse (1926) compared A. the ventrolateral spines.

Fig. 4. Protanisoceras auriculum sp. nov.; GSSA M2416, holotype, lateral view; from Algebuckina 17,

32 km SE of Oodnadatta; Oodnadatta Formation, Middle Albian; x |.

150 K. J. MCNAMARA

PROTANISOCERAS Spath 1923

Type species: Hamites raulinianus d’Orbigny

1842, p. 546, Pl. 134, figs 5-8; by original

designation of Spath 1923, p. 75.

Remarks: Spath (1939) distinguished Protani-

soceras from the morphologically similar Ani-

soceras by its smaller size, the more regularly

planar coiling and simpler suture line which

has a trifid umbilical lobe. Klinger (1976) has

noted that this lobe is smaller than the lateral

lobe in Protanisoceras, whereas he believed

that it was of similar size to the lateral lobe in

Anisoceras. The species of Anisoceras de-

scribed here shows that even in some members

of this genus the umbilical lobe may be much

smaller than the lateral lobe. However, the

trifid umbilical lobe of Protanisoceras and

bifid umbilical lobe of Anisoceras are

diagnostic.

Klinger (1976) has further noted that the

coiling and ornamentation are variable within

Protanisoceras. Both ventrolateral and lateral,

or just ventrolateral tubercles or spines may

be present; they may appear on all, or only

some, ribs. The tubercles may be connected

by one or more ribs, Furthermore, the orna-

mentation on the recurved crozier may vary

considerably from the shaft.

Casey (1961) regarded P. nodosum as

belonging within a separate genus, which he

named Heteroclinus, on account of its ‘button

and loop’ ornament. Klinger (1976) has pre-

ferred to regard Heteroclinus as a synonym of

Protanisoceras as species such as P. parce-

tuberculatum Collignon show intermediate

characters between Protanisoceras and Hetero-

clinus in possessing both single and looped

ribs. This situation also occurs in one of the

Australian species described below.

Protanisoceras auriculum sp. nov.

FIGS 4, 5, 6B, 9A-—C

Etymology: Latin—auriclum—ear; pertaining

to the shape of the shell.

1966 Labeceras (Appurdiceras) cordycepoides

(Etheridge) (pars.); Ludbrook, p. 190.

1966 Myloceras axonoides (Etheridge); Lud-

brook, pp. 44, 190 (pars.), Pl. 28, fig. 1.

Holotype: GSSA M2416, part of the phragmo-

cone and body chamber (Figs 4, 5A); from

Oodnadatta| Formation, Algebuckina 17

(5/571/17) (Ludbrook 1966), 27°492’S,

135°344’E, 32 km SE of Oodnadatta, S.A., on

North Creek, near its junction with Neales

River (OQODNADATTA 1:250000 geological

map sheet).

Paratypes:; GSSA M2444, 3546, from the

same locality as the holotype and M3547 from

Toodla 8 (5/561/8), 3 km SW of Mt Arthur,

27°31°S, 135°41E,

Other material: In addition to the type speci-

mens, 12 further specimens are known: GSSA

M2446, 2454, 3548-3556 from Algebuckina

17 and M3061, 3557 from Toodla 8.

Age; Middle Albian.

Diagnosis: Coiling aspinoceratid. Ventrolateral

tubercles occur infrequently on single ribs on

early phragmocone and late body chamber;

occur more frequently on later phragmocone

and early body chamber where may cover two

or three ribs. Ribs broad and widely spaced on

early phragmocone; becoming finer and more

closely situated adaperturally.

Description: Phragmocone forms open coil

throughout. Whorl section ovoid throughout,

whorl height slightly greater than whorl width.

At earliest known part of phragmocone (Fig.

SE) at whorl height of 4 mm, ornament con-

sists of simple, non-tuberculate, slightly pror-

siradiate ribs. At this stage there are four ribs

in a distance equal to whorl height. At slightly

greater whorl height every fifth or sixth rib is

flattened across venter and small tubercles

occur ventrolaterally. Up to a whorl height of

9 mm ribs become increasingly prorsiradiate;

ribs more strongly inclined toward dorsum.

Tubercles at this whorl height occur more

frequently and become elongate, spreading

across two ribs; up to two intercalated non-

tuberculate ribs. Across venter ribs form loop

between tubercles and on latter part of phrag-

mocone form swollen band. Tuberculate ribs

may also form swollen band on flanks. At

whorl height of 10 mm tubercles may cover

three ribs and be separated by only one or two

intercalated ribs. Ribs on dorsum pass straight

across and are weaker than on flanks, Between

whorl height 14 mm and 26 mm ribs become

more rectiradiate. At whorl height of 30 mm

there are 11 ribs in a distance equal to whorl

height.

Body chamber commences at whorl height

of 32 mm. Tubercles become more widely

spaced, covering 2-3 ribs being separated by

up to 7 intercalated ribs. Last large tubercles

occur at whorl height of 41 mm. Tubercles

may become spinose on early body chamber,

but progressively decrease in size adapertur-

ally, covering only one rib but occurring on

every rib. On body chamber ribs become almost

rectiradiate; they become increasingly sinu-

ALBIAN HETEROMORPH AMMONITES 151

Fig. 5. Protanisoceras auriculum sp. nov.; A, GSSA M2416, holotype, ventral view; B, GSSA M2444,

paratype, lateral view; GSSA M3547, paratype, C, lateral view, D, ventral view; E, GSSA M3550,

lateral view. A, B, E from Algebuckina 17, 32 km SE of Oodnadatta; C, D from Toodla 8, 3 km

SW of Mt Arthur; all Oodnadatta Formation, Middle Albian; all x 1.

soidal adaperturally. Body chamber reaches a

maximum known whorl height of 50 mm.

Suture line with broad, bifid lateral lobe and

small, trifid umbilical lobe, half width of

lateral lobe; internal lobe trifid (Fig. 6B).

Discussion: Klinger (1976) has expanded the

concept of Protanisoceras to include those

forms which have tubercles spreading across

more than one rib. This looped ornament, so

well developed in P. auriculum, is seen in the

European Joricatus Zone (mid-Middle Albian)

P. nodosum and P. flexuosum (d’Orbigny). P.

auriculum can be distinguished from these

species by its more elongate tubercles which

extend over a greater number of ribs on the

phragmocone, more prorsiradiate ribs and less

ornamented body chamber. The Madagascar

species P. parcetuberculatum Collignon (1962),

like P. auriculum, possesses both single and

looped ribs. It can be distinguished from P.

auriculum by its narrower ribs and smaller

tubercles.

Protanisoceras gracile sp. nov.

FIGS 6A, 7, 9D, E

Etymology: Latin

1966 Labeceras (Appurdiceras) cordycepoides

(Etheridge) (pars.); Ludbrook, p. 190.

1966 Myloceras axonoides (Etheridge) (pars.);

Ludbrook, p. 44.

eracilis—slender.

(52 kK. 1. McNAMARA

Hololype; GSSA M2455, from Oodnadatia

Formation, Algebuckina 17 (5/571/17) (Lud-

hrook 1966), 27°494’S, 135°344°E, 32 km SE

of Oodnadatta, on North Creek, near its

junction with Neales River (OODNADATTA

1:250 000 geological map sheet),

Paratypes: GSSA M3558 from same locality

as holotype and M3059 from Toodla 8, 3 km

SW of Mt Arthur,

Other material: GSSA M2449, 3560-3567

from Algebuckina 17 and M3568-3569 from

Toodla 8.

Ape: Middle Albian.

Diagnosis; Coiling ancyloceratid; whorl see-

tion ovoid, Ventrolateral tubercles infrequent,

occurring only on shalt and restricted to single

ribs. Ribs prorsiradiate throughout, except on

recurved hook where become rectiradiate

adaperturally.

Description; Earliest known part of phrag-

mocone with whorl helght of 3 mm; mod-

crately strongly coiled; with single, non-tuber-

culate, gently prorsiradiate ribs. Tubercles first

uppear al whorl height of 9 mm as small

prominences either side of siphonal line. On

early part of shaft tubercles occur on about

U L E

fo 3s animes

Ves Soe at : r

UP Ww) aa

\ 2 vA

| i |

70mm

every sixth rib. At Whorl height of 10 mm ribs

become sinuously prorsiradiate, more strongly

inclined toward dorsum. Ribs thicker and

more widely spaced along shaft. At whorl

height of 12-14 mm small tubercles present on

all ribs in some individuals, but Jess frequently,

or not at all, on others, On recurved body

chamber tubereles absent. Adaperturally ribs

on body chamber wider and rectiradiate.

Whorl section ovoid throughout shell with

width §2% whorl height, with maximum whorl

height on recurved body chamber uf 19 mm,

Suture line like that of P. auriculam.

Discussion; P, gracile can be easily distin-

guished from P. evriculum by its smaller size:

possession of a shaft; weaker tuberculation;

absence of looped nbs and. slightly smaller

lateral lobe. P. gracile is most similar to P.

nodaxum from the Middle Albian /ericatus

Zone in southern England in lacking lateral

tubercles and having ventrolateral tubercles

which do not occur on all ribs, P. gracile

differs in its lack of looped ribs, tubercles

Which are not spinose, possession of more

strongly prorsiradiate ribs and absence of

luberculation on the body chamber. #&

flexuosum, also from the Joricatuy Zone, simi-

Fig. 6, Suture lines of: Ay Protunisoecras gracile 8p. noy., GSSA M2455, holotype, at whorl height of

12.5 mms BL P. avricuham sp. noy.,

GSSA M3546, paratype, at whorl height of 16 mm; C, Proiani-

soceray sp. B, NMV_ P52327, at whorl height of 14 mm; D, Anisoceras sweeti sp, nov. NMV

P52328, holotype, at whorl height of 23 mm, 1 — inlernal lobe; U = umbilical lobe: L

lateral lobe:

ALBIAN HETEROMORPH AMMONITES 153

Fig. 7. Protanisoceras gracile sp. nov.; GSSA M2455, holotype, A, lateral view, B, ventral view; C,

GSSA M3059, paratype, lateral view; GSSA M3558, paratype, D, lateral view, E, ventral view;

A,B,D,E, from Algebuckina 17, 32 km SE of Oodnadatta, C from Toodla 8, 3 km SW of Mt Arthur;

all from Oodnadatta Formation, Middle Albian; all x 1.

larly lacks lateral tubercles and possesses only

small ventrolateral tubercles like P, gracile;

however in P. flexuosum they occur more

frequently.

P. gracile is similar to some species from the

English Early Albian mammillatum Zone,

such as P. raulianum (d’Orbigny), P. canti-

anum (Spath) and P. blancheti (Pictet & Cam-

piche). These species, like P. gracile, possess

only ventrolateral tubercles and lack looped

ribs, However, P. gracile can be distinguished

from these species by its more strongly pror-

siradiate ribs. P. gracile resembles P. gradatum

Collignon (1963, p. 40, Pl. 256, fig. 1101)

from the Early Albian of Madagascar, but it

is smaller and possesses more inclined ribs.

Protanisoceras aff. gracile sp. nov.

FIGS 8, 9F

Material and locality: One specimen, GSSA

M2441, from Oodnadatta Formation, Alge-

buckina 17 (5/571/7), 32 km SE of Oodna-

datta (OODNADATTA 1:250000 geological

sheet map).

Age: Middle Albian.

Remarks: This specimen, consisting of the

latter part of the shaft and the recurved body

chamber, differs from P. gracile in the pos-

session of tubercles which extend across two

ribs on the latter part of the phragmocone.

Like P. gracile the body chamber lacks tuber-

culation; however, the tighter recurving of the

body chamber has resulted in the umbilical

bifurcation of some ribs. In terms of whorl

section and size this specimen conforms with

P. gracile, but its more strongly developed

tuberculation and tighter recurving are dis-

tinctive.

Protanisoceras sp. A

FIGS 9G, 10A, B

Material and locality: An incomplete shaft,

NMV P60543, from “Primrose Springs, Peake

Station”.

Age: Middle Albian,

Description: Whorl section circular with dia-

meter of 16 mm. Ribs slightly prorsiradiate;

each rib bears small ventrolateral and lateral

tubercle. Tubercles cover only single rib. There

are eight ribs in a length equal to whorl dia-

meter,

Discussion: This form can be easily distin-

guished from P. sp. B by the absence of looped

ribs with tubercles covering more than one rib,

154 Ke Ts

McNAMARA

Fig. 8. Protanisoceras aff, gracile sp. nov.; GSSA M2441, A, lateral view, B, ventral

view; from Algebuckina 17, 32 km SE of Oodnadatta; Oodnadatta Formation, Middle

Albian; both x 1.

The absence of suture and the impression of

the dorsum of the phragmocone on the matrix

attached to the specimen indicate that the

specimen is the recurved body chamber. It is a

much longer body chamber than possessed by

other Australian species of Protanisoceras of

similar size. The ribbing is finer and more

closely spaced than seen in English Early-

Middle Albian species. The Middle Albian P.

cantianum Spath (1939) from southern

England has a similar whorl section and tuber-

culation, but it possesses thicker, more widely

spaced ribs.

Protanisoceras sp. B

FIGS 6C, 9H, 10C, D

Material and locality: A single, incomplete

phragmocone, NMV P52327, from ‘‘Primrose

Springs, Peake Station”.

Age: Middle Albian.

Description: This specimen, an incomplete,

largely internal mould of the latter part of the

phragmocone, is characterised by possession of

large ventrolateral and lateral tubercles of

similar size. Tubercles connected by looped ribs

and extend across three ribs; separated by 0—2

intercalated non-tuberculate ribs. Whorl section

is semicircular. This form particularly charac-

terised by large, bifid lateral lobe (Fig. 6C)

which is almost half as wide again as first

saddle; it is four times wider than_ trifid

umbilical lobe.

Discussion: Specimens of Protanisoceras

described by Klinger (1976) from Zululand

also possess both ventrolateral and lateral

tubercles. However, in all the forms

Klinger described the tuberculate ribs are

much more widely separated by non-tuber-

culate ribs than in the S.A. forms. P. sp. B

compares with some English Late Albian

species of Anisoceras, such as A. armatum,

in the nature of the tuberculation; however,

whereas species of Anisoceras possess a bifid

umbilical lobe it is trifid in P. sp. B. The

ornamentation is like that of A. sweerti. The

two species can be distinguished by the nature

of the umbilical lobe and the smaller size of

P. sp. B. This species differs from P. auriculum

and P. gracile in its possession of lateral

tubercles.

Family HAMITIDAE Hyatt 1900

HAMITES Parkinson 1811

Type species: Hamites attenuatus J. Sowerby

1814, by subsequent designation of Diener

1925, p. 65.

Hamites cf. attenuatus J. Sowerby 1814

FIG, 11

Material and localities: A complete body

chamber, NMV_ P52336 from ‘Primrose

Springs, Peake Station”, and an incomplete

body chamber, GSSA M2447, Oodnadatta

Formation, Algebuckina 17 (5/571/17).

Age: Middle Albian.

Remarks: The well preserved body chamber

has an almost circular whorl section. Like H.

attenuatus from the Middle Albian dentatus-

ALBIAN HETEROMORPH AMMONITES 155

Fig, ¥, Diagrammatic representation of variation in distribution of ribs and tubercles in species of

Protanisoceras. A-~C, P. auriculum sp. nov., A, GSSA M3550, B, GSSA M3547, paratype, C, GSSA

M2444, paratype; D-E, P. gracile sp. nov., D, GSSA M3558, paratype, E, SADM M2455, holo-

type, F, P. aff, gracile sp. nov., GSSA W2441, G, PF. sp. A, NMV P60543; H, P. sp. B, NMYV P52327,

All natural size.

loricatus Zones of southern England, the

S.A. form possesses ribs which are slightly

prorsiridiate prior to the hook; rectiradiate

on the hook, becoming initially rursiradiate

on the recurved shaft, then finally rectira-

diate. Similarly it has 7-8 ribs in a length

equal to the whorl diameter. The whorl section

of the English form is said to be slightly

laterally compressed (Spath 1939) whereas it

is slightly dorsoventrally compressed in the

S.A. form.

In both forms the adapertural part of the

body chamber curves away from the phragmo-

cone, The impression of the dorsum of the

phragmocone against the body chamber (Fig,

111A) shows that the body chamber was

deflected away from the phragmocone during

growth as the two shafts came into contact.

The suture line of the $.A. form is of similar

proportions to the English form, with a bifid

lateral Jobe and small trifid umbilical lobe,

Whitehouse (1926) described a torm from the

Albian of Qld which he called A. aff. maxi-

mus J. Sowerby. This specimen, as can be seen

in’ Whitchouse’s figure, possesses a trifid

lateral lobe, whereas in Hantites it is bifid:

it iy thus not a species of Hammites.

Age of the ammonites

The Marree Subgroup comprises the Aptian

Bulldog Shale and the Albian Oodnadatta

Formation (Freytag 1966, Ludbrook 1966,

1978, 1980). Since Ludbrook’s (1966) bio-

stvatigraphical study was submitted for pub-

lication, the OODNADATTA 1:250 000 geo-

logical map sheet has been published (Freytag

et al. 1967) and the rock units comprising the

Aptian-Albian sequence named in some detail

(Freytag 1966). It is now possible to relate the

ammonites to the rock units, as mapped on the

OODNADATTA and adjoining sheets, from

which most of them were collected.

The ammonite Sanmartinvceras (Sinzovia)

/ontinale from the Marree Subgroup at *Prim-

rose Springs, Peake Station’ was described by

Hudleston (1890), Thomson (1974) discussed

the range of Sanmartinoceras and believed

that it is, by and large, an Aptian form, The

oecurrence of S. (Sinzevia) in association with

Tropaeum in Qld led Day (1969) to conclude

156 K. J. MCNAMARA

Fig. 10. Protanisoceras sp. A; NMV P60543, A, lateral view, B, ventral view.

Protanisoceras sp. B, NMV P52327, C, lateral view, D, ventral view. Both from “Primrose Springs,

Peake Station”; Oodnadatta Formation, Middle Albian, both x 1.

Fig. 11. Hamites cf. attenuatus J. Sowerby 1814; A, lateral view, B, ventral view;

from “Primrose Springs, Peake Station”; Oodnadatta Formation, Middle Albian;

x 1. Arrow indicates impression of dorsum of part of phragmocone.

a Late Aptian age for the genus in Australia.

A Late Aptian age for part, at least, of the

Bulldog Shale is further indicated by the

presence of Tropaeum in S.A. (Howchin &

Whitehouse 1928).

In her biostratigraphical study of the

Cretaceous rocks of the Great Artesian Basin

in S.A. Ludbrook (1966) concluded that

there was no reliable means of establishing a

detailed biostratigraphic zonation of the

ALBIAN HETERDMORPH AMMONITES 157

Marree Suheroup between the Late Aptian

and Late Albian an the evidence of animonites.

Part of the reason for this hus been the aftribu-

tion of any small heteromerph ammonite

{ound in the formation to the Late Albian

genera Myloceray or Lubeceras (eg. Lod-

hrook T8966), although it has naw been shown

Unat a numbec of other geners ave present. Ut

wiso stems from the inaccurate stalement of

Brunnschweiler (1959) who, in deseribing

species of Falcitereiia tram the Santos Oodna-

datta Wo. 1 Well, stated, “The heds from the

surface dowh to about 375 fect contain also

Myloceray, Labeceras, Appurdiceras, Bolire-

cerus ete, and are to he regarded as early

Upper Albian - -) Palciferella he recorded

hetween 71,5 m (235 ft) and 113.3m (372 ft)-

Vhis icd Bninnschweiler to conclude that

fuleiferclla was of Late Albian age in

Australia (even though it is resericted ta the

Mickle Albian interinedtus afl niobe Sub-

zones of the favicatas Zone in England (Owen

1971)) as the Lebeecrays—-Myluceras faana in

Old, Madagascar and Zululand has been

established as Late Albian (Whitchouse 1926,

Klinger 1976, McNamara 1978). However, as

Ludbrook (1966) has noted, this Late Albian

latina does not occur with Fuleiferella in the

Oodnadatta No. | Well. Brunnschwelller was

probably referring to the Late Albian

ammonite fauna of Fossil Creek (Reyment

YA aly).

Ludhrook (19667 ploced the “unnamed green-

sand member” (now the Coorkiina Member

of the Oodnadathe Formation), which ovenrs

in Santos Oodnadatta Na, 1 Well between 13)

and 137 m, ar the base of the Albian, She

records Falciferclla in the well between this

member and the lop of the Oodnadatta Forma-

tion, Which is thoughe to be of Late Albian age

(Ludbrook 1978), at bout 91 om, This is sug-

veslive of a Midle Athian age for Faleiferelfa

in Australia as in Eneland,

Cooper & Kennedy (1979) have recently

placed the two deseribed Australian species

F, hreadent and F. reymenti, im the binneyitid

Norissiakareras, which, apart from an tmacom-

plete specimen feom the uppermost Albian

of Angola, is restricted to the Late Cero-

manian to Early Turonian (Wright ta Arkell

+f al. 1957), Cooper & Kennedy consider that

jhere is a qlircet phylogenetic relationship

belween the Middle Albian Falciferclia, with

its Faleoid growth lines and ribs. and the almost

smooth Berissiakeceras. Following Brunn-

schweiler's assignment of 4 Late Albian age to

BP. hreadent and FP. reymenii, Cooper &

Kennedy suggested that these species may

helons in Borisstakoceras, However, these

species, like the type species of Fulciferclla, F,

millbaurnei Casey (1954), have tine ribs on

the body chamber. and a trifid lateral lobe,

which in Borissigkoceray is bifid (Cobban

1961), Examination of the type and topotype

material of F. breadeni fram the Qodnadatra

Formation, reveuled the suture line to be more

erenulate than shawn by Brunnschweiller

(1959), being very close to that af £, mill-

bourne’. Furthermore the occurrence of F,

hreaden’ and FF. reymenti with the Middle

Albin species af Pratanivaceras (see below)

and a Middle Albian species of Marites, and

possessing Tibbing which 35 more akin to Fal-

ciferella than to Borissiakoceray, Sugeest that

Brunuschweilers ariginal emplacement in

Falciferella is) more appropriate. Obviously

there is a close relationship between these two

genera, sufficient for Kennedy & Juignet

(1973) to have placed Fale‘/eretla in the

Binneyitidae anc not the Oppeliidac os did

Wright (in Arkell e¢ al 1957),

At Algebuckina 17 Faletferella occurs (Lud-

hrogk 1966) with Protanisaceras auriculiin

und P. yraete. Speeies of Protanisacerey alse

occur at “Primrose Springs, Peake Station’.

Protanisoceras was considered by Wright (in

Arkell et ei. 1957) io range from the Early-

Middle Albian. “The yougest species in the

English Middle Albian aceurs in the inivr-

inediny Subzone of the foricaray Zone (Qwen

1971), Klinger (1976) extended its lower

range into the Lale Aptian. Casey (1861) has

shawn thal the vurliest English Albian speeies

of Pretanisoeeras, whieh appear im the

flortdion Subzone of the manmilldtian Zoe,

compare closely with cantemporancous species

ul Mamites, differing only in the develop-

ment of small vertrolateral tubercles which

cover single ribs, In the succeeding rau/fanun

und pucianus Subzones there is a general trend

toward inereasing tuberculatian, the species

possessing more Frequent and prominent ven-

trotateral tubercles and the development of

lateral tubercles! these species coexist with

poorly tuberculute species, In the early Middle

Albian dentures and early Jorfearuy Zones

(Spath L939) species with lateral tubercles

predominate. and an increasing number of

species, sich as FP. nodes and P, flexvasum

oF the foricatis Zone (Owen 1971), have

looped rihs. In these Tnfer species there is a

loss of lateral tubercles. as oceurs in PL auricu-

lum and P grecile.

158 kK. J, McNAMARA

The occurrence at Algebuckina 17 of species

of Protaniseceras morphologically closest to

the Jericatis Zone species, coexisting with

species of Falciferella, which oeeurs only tn

the first two subzones Of the loricarus Zone

(Owen 1971), and with Mamites cf artenu-

alas, Which ranges from the late deratus Zone

through the /oricatus Zone, suzeests that this

part of the Godnadatta Formation may cor-

relate with the mid-Middle Albian Jertcunes

Zone of the Angzlo-Paris Basin-

The locality cited as “Primrose Springs,

Peake Station” in the old literature probably

includes more than one locality, ws stated

above, Until the WARRINA 1:250 000 geo-

logical map sheet is mapped in detail, it will

not be possible to identify the precise localitics

From which the Late Aptian Sanmerrinoceras

(Sinzevia) fontinale, and the Middle Albian

species of Pretanixoceras with looped cibs aud

Hanites cf. atretuatus, were collected In

audition, the occurrence of Anisocéras sweetl

indicates that younger strata also outerop in

this region. ws dhe genus ranges from the Late

Albian to the Late Turonian (Wright in Arkell

et al. (957). As the Blanchewater Formation

Which o¥erlies the Marree Subgroup in the

Marree area is thought to be latest Albian in

age, possibly extending into the Cenomanian

(Ludbrook 1966, 1978), the upper part of the

Oodnadatla Formation is early Late Albian in

age. This has been established at Fossil Creek

by the presence of My/oceras and Labeceras,

Acknowledgements

1 thank Mr J. M. Lindsay (GSSA), Mr N-

§. Pledge (SAM) and Mr T. A. Darragh

(NMY) for the loan of specimens; Dr N, H,

Ludbrook for drawing to my attention the

existence of the GSSA specimens and provid-

ing information on the sttatigraphy; Or W, J.

Kennedy (Oxford) for kindly assisting me

with literature; and Miss Val Ryland for

photographing the specimens,

References

ARKELL, W. J,, KUMMiL, B, & Wri, G, W,

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(195L) A monogruph of the Ammonoiden of

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Day. R. W. (1969) The Lower Cretaceous of the

Great JArtesian Basin. Jn K. 5. W. Campbell

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ar 20. dinmanolded neacretaven. (Bertin,

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ontology of South Australia. No. 14—Creta-

ccous fossils from Dalhousie Springs. Parl. Pap-

S, Aust, Ti, 13-17.

(1909) Lower Cretaceous fossils from Uhe

sources Of the Bureoo. Ward and Nive Rivers,

south centrul Queensland. Pi. 2, Cephalopoda

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‘marine Lower Cretaceous sediments in the Ood-

nadatts tegioti af the Great Artesiun Basin.

@. geal Notes, Geol. Surv. S. Aust. 18, 3-7.

——, Heats, G. R. & Worrnver, H, (1967) DOD

NADATTA map sheel, Geological Atlas of

Pa Austealia, 12250 000 series Geol Surv,

S. Aust.

Howie, Wo & Worerinose, F, W. (1928) A

new and very large cnocerulid ammonoid From

the Cretaceous of centrul Australia Ree. 8.

Ausi. Mes. 3, 483-492.

Huprestor, W. H, (1890) Further notes on some

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ALBIAN HETEROMORPH AMMONITES 159

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AGES AND ASHES IN LAKE FLOOR SEDIMENT CORES FROM VALLEY

LAKE, MT GAMBIER, SOUTH AUSTRALIA

BY C. E. BARTON & M. W. MCELHINNY

Summary

A set of our cores from Valley Lake shows a sequence of fresh water organic muds above a band of

argonite 8-10 cm thick, overlying a graded calcareous tuff. Magnetic remanence and susceptibility

measurements indicate the absence of volcanic episodes since the onset of deposition of the organic

muds 5000 to 6000 years ago. Radiocarbon ages of ~14 000 years and ~38 000 years for the

aragonite band and the tuff respectively are not considered to reflect their ages of formation.

AGES AND ASHES IN LAKE FLOOR SEDIMENT CORES FROM VALLEY

LAKE, MT GAMBIER, SOUTH AUSTRALIA

by C. E. Barton*+ & M. W. McELHINNY*

Summary

Barton, C. E. & MCELHINNy, M. W. (1980) Ages and ashes in lake floor sediment cores

from Valley Lake, Mt Gambier, South Australia, Trans. R. Soc. S. Aust. 104(6), 161-165, 28

November, 1980.

A set of four cores from Valley Lake shows a sequence of fresh water organic muds above

a band of aragonite 8-10 cm thick, overlying a graded calcareous tuff. Magnetic remanence

und susceptibility measurements indicate the absence of volcanic episodes since the onset of

deposition of the organic muds 5000 to 6000 years ago. Radiocarbon ages of ~14 000 years

and ~38000 years for the aragonite band and the tuff respectively are not considered to

Teflect their ages of formation.

Introduction

Valley Lake (37° 51'S, 140° 46’E) is the

second largest of the four lakes in the Recent

volcanic craters at Mount Gambier, South

Australia. Chemical and biological aspects of

the lake have been described by Bayly & Wil-

liams (1964), and the morphology and benthos

by Timms (1974). The lake is now fresh and

at a level considered to be controlled by the

ground water table.

The geology of the Mt Gambier complex

has received considerable attention, the most

recent being a detailed study by Sheard (1978)

which includes a review of the previous work.

In Sheard’s reconstruction the two larger lakes,

Blue Lake and Valley Lake occupy open

craters called maars, formed by volcanic ex-

plosions, as do the smaller lakes, Brownes

Lake and Leg of Mutton Lake.

Two charcoal samples picked from soils

beneath tuff layers have been radiocarbon

dated. The first was collected by C. G. Stephens

in the township of Mt Gambier and dated

at 4830 + 70 BP (Gill 1955; Fergusson &

Rafter 1958), and the second was collected

4 miles away to the SSE and dated at 1410

+ 90 BP (Blackburn 1966). Blackburn was

of the opinion that these dates may represent

separate volcanic episodes, and this view has

also been adopted by Sheard (1978).

Four cores were recovered in 54 mm (class

12) PVC tubes using a 6 m Mackereth corer

(Mackereth 1958): VB in 16 m of water

from the deepest part of the lake, and VA, VC

* Research School of Earth Sciences, Australian

National University, P.O. Box 4, Canberra,

A.C.T. 2601.

* now at: Geophysics Department, Edinburgh

University, U.K.

and VD in 14.5 m of water from the flattish

area about 50 m NE of the deepest part (see

Timms (1974) bathymetric chart). Echo

soundings showed small scale variations in

bottom topography not resolved in Timms’

chart; cores were collected as close as possible

from the hollows.

Core descriptions

All four cores displayed the same features:

approximately 1 m of black fresh-water organic

muds, above a very clearly defined 8-10 cm

band of extremely fine grained creamy white

aragonite, overlying a graded column of cal-

careous tuff. VD achieved the maximum

penetration through the tuff and is pictured in

Figure 1.

Shells are abundant in the organic muds

and were identified by B. J. Smith as “. . .

assemblages of ostracod shells and the small

freshwater bivalve Pisidium sp. These are

found in fresh waters low in dissolved salts

and usually permanent.”

X-ray analysis of the creamy white band

performed by J. Caldwell of A.N.U., gave a

composition of 95% aragonite + 5% low

magnesium calcite. Under the microscope

much of the material consisted of rods ~1 pm

in length. Diatoms were common and, in

contrast to the underlying tuff, there was a

marked absence of quartz and ferromagnesian

(opaque) minerals,

The graded tuff was rich in carbonates

with some euhedral rhombs (calcite/ dolomite)

but mainly irregular fragments. Volcanic

glass, angular with inclusions of crystallites

and gas bubbles, was common. Quartz grains,

usually fairly well rounded, were present to-

gether with a scattering of microfossils.

(50

160

240°

260

(90

270

200

210

Fig. 1. Photocomposite section through Valley

Lake core VD. Distances from top of core

given in cm.

Evidence of horizontal bedding occurred in

the top 10 cm of the tuff column, but other-

wise the material appeared to have been rapidly

deposited under water. The boundary with the

aragonite band was less abrupt than that

between the organic muds and the aragonite,

but nevertheless quite sharp, as can be gauged

from the photograph.

J. R. Dodson examined samples from the

aragonite band and the upper calcareous tuff

for pollen grains. In the aragonite there were

plenty of grains, particularly Casuarina and

Eucalyptus with some aquatic taxa, whereas

the tuff contained very few grains: a scattering

of Casuarina and Eucalyptus but no Com-

positae, Although insufficient material was

examined to provide a definitive conclusion,

these assemblages are consistent with a Holo-

cene age for the aragonite and preclude an

. BARTON & M. W. McELHINNY

age greater than 15 000 BP for the deposition

of the tuff, which must have occurred rapidly

(Dodson pers. comm.).

Magnetic results

Measurements of the horizontal natural

remanent magnetisation (NRM) were made

at 1 cm intervals along the length of each

complete core using an automated version

(Barton 1978)! of the “Digico” whole core

spinner magnetometer (Molyneux et al. 1972).

VD was sliced open, subsamples were extracted

in adjacent pairs of perspex cube shaped pots

(volume 5,3 cm") every 2.5 cm, and measured

on a _ cryogenic “SQUID” magnetometer

(Goree & Fuller 1976).

All cores yielded mutually consistent results,

showing a large contrast in NRM_ intensity

between the organic muds (typically 0.5—1.5

mA.m!) and the calcareous tuffs (typically

100-180 mA.m-) as illustrated in Figure 2.

A well dated magnetic secular variation pat-

tern exists for SW Victoria covering the last

1000 years based on the magnetic remanence

of sets of cores from L. Keilambete, L. Bullen-

merri and L. Gnotuk (Barton!). Unfor-

tunately, the directional results from Valley

Lake (Fig. 2) are too scattered to permit

magnetic dating. Magnetic cleaning in an alter-

nating magnetic field (AF) of peak value 15

mT failed to reduce the scatter. Median de-

magnetising fields (i.e. the peak AF required

to halve the initial remanence) for 8 specimens

distributed throughout core VD ranged from

2 to 6.5 mT, which is too low to sustain a

stable primary remanence. The high water

content in the organic muds (85-90% by

weight) certainly contributes to this instability.

Initial susceptibility measurements on core

VD (Fig. 3) reflect a contrast of about 3

orders of magnitude between the organic muds

and the calcareous tuffs. Much of the organic

mud is weakly diamagnetic, i.e. the suscepti-

bility is negative.

Radiocarbon dating

An initial radiocarbon age of 38400 BP

on the total organic fraction from VD 107—

117 cm prompted a more detailed investigation

into the chronology of these cores. The results

are given in Table 1. Both the calcareous tuff

1 Barton, C. E. (1978) Magnetic studies of some

Australian Lake Sediments. Ph.D. thesis (un-

publ.), Australian National University,

Canberra.

LAKE FLOOR SEDIMENT CORES MT GAMBIER

(cm)

CORE

DEPTH

Ww DECLINATION E

INCLINATION

163

CORE VDNRM

INTENSITY (MA /M)

Fig. 2. NRM results for core VD. Vertical grid interval (bar spacing) is 20 cm; pairs of measurements

at same stratigraphic level linked by lines. Above 20 cm core was 100 wel lo be subsampled; whole

core measurements showed that intensity remained low in this zone.

and the aragonite band yielded barely sufficent

organic carbon to obtain a date, hence the

large counting uncertainties. A carbonate date

was obtained for the aragonite band in VA.

Radiocarbon ages are plotted against the

equivalent distance from the top of VB in

Figure 4, Correlation between YD and VB

for sample ANU 1809 is based on equal

sedimentation rates within the tuffs and may

therefore be in error by up to say + 5 cm;

there can be no uncertainty about the equiva-

lent position in VB of the aragonite band,

sample ANU 2051.

Within the organic muds, the monotonic

MC age sequence is consistent with uniform

deposition since 6000 BP, The fact that the

MC ages within the organic muds plotted in

Figure 4 extrapolate to near the origin is taken

to indicate the absence of any major systemutic

increase in ages due to the incorporation of

ancient carbon (from say, the Miocene lime-

stone basement which outcrops around parts

of the lake). Although further age determina-

tions are really requred to confirm this, it is

worth noting that no systematic age increases

in excess of a few hundred years have been

164

OF CORE VDODSUSC

TOP

E \oo

w —t a

c .

o hE

= a"

200

| ! 10

SUSCEPTIBILITY

loo 1000

(MICROGAUSS/ GE }

Fig. 3. Initial susceptibility results for core VD.

Format of plot is as for Fig. 2 except that

iegative (diamagnetic) susceptibilities plotted

us positive with X jnstead of square. Much of

upper 80 cm of organic muds diamagnetic.

Volume susceptibility of 1 Gauss Oersted-! in

ces equivalent to 47 in SL system and

dimensionless.

C. E. BARTON & M. W. McELHINNY

found in sequences from L. Keilambete, L.

Bullenmerri and L. Gnotuk in SW Victoria

(Bowler & Hamada 1971; Barton & Polach

1980). These lake sediments have been inten-

sively dated by radiocarbon and are from simi-

lar geological environments to Valley Lake.

Ages of eruption

The graded calcareous tuff has every appear-

ance of having been rapidly deposited in a

single episode into a lake containing at least

1-2 m water, Excluding the possibility that

this occurred 38 000 years ago, which is incon-

sistent with previous age determinations, the

pollen data, and the morphology of the Mt

Gambier complex, there must be considerable

amounts of ancient organic carbon (charcoal)

incorporated in the tuff to account for such

an age.

Intensive radiocarbon analysis of magneti-

cally correlated cores of organic mud from

Bullenmern, 38°15'S, 143°06'E (Barton!;

Barton & Polach 1980) indicates 4 25% praba-

bility of >20% anomalies in radiocarbon

ages, These muds are not dissimilar from those

in Valley Lake, Although these figures over-

estimate the dating uncertainties in many

lacustrine sequences, e.g. Keilambete, 38°13'S,

142°52’E, (Bowler & Hamada 1971; Barton

& Polach 1980), they should nevertheless be

regarded us a guide in assessing the significance

of isolated "'C. determinations. Hence the 6180

+ 80 BP age at the bottom of the organic

muds is not necessarily inconsistent with an

eruption age of 4800 BP.

Magnetic intensity and susceptibility con-

trasts between the organic muds and the tuffs

provide a sensitive measure of the presence

of yoleunic ejecta within the sequence, At no

point within the organic muds do either of these

Tati lL. Conventional radiocarbon ages for samples from three Valley Lake cores, All determinations,

Equivalent.

ANU Sample Depth in Depth in MWC age

number Core (cm) VB (em) *1SD Comment

ANU 2125 VB 40-50 40-50 2960 —& 90 Organic mud

2126 VB 80-90 73-83 3960 + 80 Organic mud

2052 VB 110-120 103-113 6180 80 Organic mud

2051 VA 117-122 114-122 13900 + 370 Aragonite (organic)

15450 > L600" Arigonite (inorganic!

1809 VD 107-151 fd 151 38400 + 2070) Calcareous tuff

1640)

" total inorganic fraction

LAKE FLOOR SEDIMENT CORES MI GAMBIER 165

REOIOCSABON AGE (Kyi

G \ i 3 + 9 6

an ’

e tb

5 KI ’ |

PS 7aH5 PLM CLP OINVEND HaLeMHSaH4

fa)

rh wf view +

awit

4) 16 +

- Jumeamy

= mele el | te ing WHITE

Ciypy abled AMEGUNITE

"7 wm | &gnk of

FE Deeetnhiray

wit ong ee

Lae 22 -

wy 2un aKad sinh ‘¢ 40)

= ec

+ o

thi

wh >

| ®

i” ’

Fig 4, Conventional radiocarbon age-depth plot

for core VB together with simplified log of core,

Ages expressed in units of 1000 years (Ky).

Vertical error bars denole sample lengths and

horizontal ones, | standard deviation counting

Uncertainties in ages. Sumples ANU 2051 und

ANU 1809, taken from cores VA and VD

respectively, murked al their equivalent dis-

lunces from top of core VB,

parameters even remotely approach the high

values within the tuffs, nor is there any eyi-

dence to the naked cye of a volcanic interlude.

It is therefore concluded with some confidence

that no eruption has occurred near the lake

since the deposition of the calcareous tufts.

The problem remains as to the significance

of the organic and inorganic ages of 14.000

years for the aragonite band, Sufficiently slow

deposition of aragonite could explain the 6000

year lime break at the upper boundary iodi-

cated by the average age of the whole band.

However, since the organic muds indicwle

fresh water conditions throughout the lust

5000 to 6000 years, it is considered improbable

that conditions under which only 95% pure

aragonite was deposited could have existed

within the lake for many thousands of years

previously, The preferred conclusion, and one

which is more consistent with the geologesl

evidence, is that the aragonite was produced

fairly rapidly at the end of the eruptive phase

at 5000 BP or possibly 6000 BP, and that both

ages reflect the presence of dead carbon derived

from the volcanic ejecta or from stirring of

the original lake floor,

Acknowledgments

We thank the Corporation of the City of Mt

Gambier for granting access to the lake and

for providing storage tacilities and information,

Dr B. J, Smith (National Museum of Vic-

ioria) for shell identification, and Dr J. R.

Dodson (University of New South Wales) for

pollen identification,

References

Baviy, | A. BE. & Witiiams, W. D. (1964)

Chemical and biological observations on some

volcanic lakes in S.E. South Australia, dust J.

Mar. Freshw, Res, 15, (23-132,

Barron, C, BE. & Potach, H. A. (1980) 14C ages

and magnetic stratigraphy in 3 Australian

muars. Radiocurbon 22 (in press).

BLAckBuRN, G, (1966) Radiocarbon dates relating

to soil development, coustline changes, and

volcanic ash deposition in south-east South

Australia, Aust. J. Sei, 29, 50-52,

Bow er, J, M, & Hamapa, T, (1971) Late Quater-

nary stratigraphy and radiocarbon chronology

of water level fluctuations in L. Keilambete,

Victoriu. Nature 232, 330-332.

Ferousson, G, J, & Rarrer, T. A. (1957) New

Feuland C age meusurements 3. NZJ. Sci.

Tech., 38B, 732-749.

Gne & OD, (1955) Radiocarbon dates for

Australian archuevlogicul and — geological

samples. Aust. J. Sei. 18, 49-52.

Goren, W. 8. & Futtor, M. (1976) Magneto-

meters using R-F driven SQUIDS and their

applications in rock magnetism und palueo-

magnetiant Rev, Geophys. Space Phys, U4, 591-

OX.

MackeretH, FP. J, H. (1958) A portable core

amet for luke deposits, Lininel. Oreanes. 3,

[81-191.

Movynnux, L., THoMson, R., Orpereco, F. &

McCartan, M. B. (1972) Rapid measurement

of the remanent magnetisalion of lung cores of

sediment. Narre 237, 42-43.

Surarp, M. J, (1978) The geological history of

the Mount Gambier volcanic camplex, soul

east South Australian. Trans. R. Soc. §. Aust

102, 125-139.

Times, B. V, (1974) Morphology and henthos

of three voleanic lakes in the Mt Gambier

district, South Australia, Anst, J. Mar. Freshy.

Rey, 25, 247-297,

AMINO ACID RACEMIZATION DATING OF LATE QUATERNARY

STRANDLINE EVENTS OF THE COASTAL PLAIN SEQUENCE NEAR

ROBE, SOUTHEASTERN SOUTH AUSTRALIA

BY C. C. VON DER BORCH, J. L. BADA & D. L. SCHWEBEL

Summary

The amino acid racemization dating technique has been applied to three selected mollusc samples

collected from the Quaternary strandline sequence of southeastern South Australia. Results of the

study are consistent with previous uranium-series age determinations in the area and imply that at

least the uppermost component of the Woakwine Range barrier-estuarine sequence was emplaced

during the last interglacial sealevel maximum around 125 000 years ago.

AMINO ACID RACEMIZATION DATING OF LATE QUATERNARY

STRANDLINE EVENTS OF THE COASTAL PLAIN SEQUENCE NEAR

ROBE, SOUTHEASTERN SOUTH AUSTRALIA

by C. C. von per Borcn,* J, L, Bava,7 & D. L. ScinwepeLt

Summary

VON pEt Boren, ©. C., BApa, J, 1. & Scuwnnet, D. L. (1980) Amino.acid racemization dating

of Late Quaternary strandline events of the coastal plain sequence near Robe, southeastern

Soulh Australia. Trans. R, Soe. S. Aust. 104(6), 167-170, 28 November, 1980,

The amino acid racemization dating techniqne has been applied to three selected mollusc

samples collected from the Quaternary strandline sequence of southeastern South Ansteulia.

Results of the study ave consistent with previous Yranium-series ave determinations in the area

and imply that at least the uppermost component of the Woakwine Range barrier-estuurine

sequence wag emplaced during the lust interglacial sealevel maxinrum around 125 OOU years

uO.

Introduction

Oxygen isotope studies of deep-sea pelagic

sediments, combined with magnetostratigraphy

and other dating techniques (Shackleton &

Opdyke 1976; Hays et al, 1976), have estab-

lished a relatively detailed chronology of

Quaternary yvlacial and interglacial stages. Re-

lated custatic sealevel oscillations recorded as

stranded shoreline deposits on continental

margins are currently under scrutiny, Although

more difficull to date, they serve as an inde-

pendent check on some of the deep sea data.

In addition, the establishment of an weceplable

chronology for Quaternary and older shoreline

sequences is of foremost interest from a geo-

dynamics point of view. A correctly dated

succession of terraces can reveal the temporal

variation in uplift rate of convergent plate

boundaries such as island ares, ad mid-plyic

tectonie movemerits such as regional warping

on passive margins. It is of interest to establish

acceptable chronologies from coastal strandlinc

sequences from a Variety of tectonic settings

and areas,

The coastal plain of southeastern South

Australia (Fig. 1) is characterized by what

may be one of the most complete and best

preserved gequenees of Quaternary strandiines

in existence. At least 20 emergent shorelines,

consisting of stranded calcarcous sand barriers

and associated lagoonal and lacustrine Ueposits,

occur in a region 9U km wide by about 400

km long (Fig. 1). A sequence of less obvious

* School pf Earth Sciences, Flinders University

of South Australia, Bedford Park, S. Aust. 5042.

+ Seripps fastinion of Oceanography and Lnstl-

tudor of Mating Resourees, Cahfornia,

+ Esso Australia Lud, Sydney,

siliceous sand beach ridges of Plio-Pleistocene

age (not shown in Fig. 1) extends for a further

100 km east of the Naracoorte Range into the

State of Victoria (Hills 1960; Blackburn et al.

1967).

The calcareous strandlines shown in Figure

| owe their preservation to a combination of

guaieaas

Pender begeonel-

Lacuttiine Factor (Fletey

Bench Dune Facies triduest

ath AWery

Uy) Revita Send

ore

Gambrer Linve erane

Volcan(Gs- 05h & babat®

jl bate Comogare vue

Grarilic juchs Early Petaeadois

9 10 20 soni

Fly, 1. Coastal Plain, southeastern South Australia,

showing Quaternary strandlines; section X-Y

refers to Figure 2.

168 Cc. GC yon der BORCH, |. L, BADA & D. L. SCHWEBEL

factors, the dominant of which has been gentle

regional upwarping of the coastal plain

throughout the Quaternary, centred on the

volcanic region in the extreme southeast of the

state (Hossfeld 1950; Sprigg 1952). This up-

warping has been responsible for the stranding

of the sequence, in which oldest shorelines in

yeneral lie furthest inland. Preservation of

these strandline features has been due largely

to rapid “case-hardening™ of the calcareous

barrier facies sands by extensive calcrete

development which generally begins imme-

diately the sands become stabilized by vegeta-

tion. Only high sealevels are represented in the

record, due to a combination of relatively slow

uplift rate and the dynamics of sediment trans-

port as sea Jevel rises from # low stillstand.

In common with other Quaternary shoreline

successions of this type, the establishment of

chronological sequence and absolute age of

individual strandlines is fraught with difficul-

lies, Palacomagnetic studies of cores from

recent stratigraphic drilling suggests that the

oldest component of the complex Naracoorte

Range barrier, shown in Figure 1, is older than

the Bruhnes-Matuyama magnetic reversal at

720 000 years; all ridges to the southwest are

younger (Cook et al. 1977). Limited radio-

carbon dating of the youngest deposits in the

sequence reported by Blackburn (1966), von

der Borch (1976), Cook er al, (1977) and

Schwebel (1979)! has established a preliminary

chronology of Holocene and late Pleistocene

sediments from lagoonal and lacustrine areas

near the present coast. Uranium-series dating

techniques have been applied to aragonitic

lagoonal sediments and molluscs dating back

to the [ust interglacial high sealevel (Schwebel

1979)),

This paper reports an initial application of

the amino-acid racemization (AAR) dating

technique (Masters & Bada 1978) to the prob-

lem of deciphering the chronology of some

aspects of the Woakwine strandline region

shown in Figure 1, It serves as an independent

check on uranium series dates obtained from

—_

x WOAKWINEYVRANGE Y

ROBE

RANGE LAKE

HAWODON

LAKE B

SICLAIR =

10 7

a oy a

QF Mere ll eer RRE See So S05 s tase cP 232s geet esse ®, Ae mele |e Teele. | #3 oto ed

= Fivaipagecs 6

Beach—-Lune Caleareous Sand

i) Amino Acid Dating Sample

QUATERNARY P| Estuarine-Lagoondal Calcgrequa @ Location

SEQUENCE Muddy Sand

Boundaries of Quaternary

Lacustrine Calcareous, Muds \ Transgressive~Regressive

Cycles

locations of samples A, B and €,

Fig. 2. Section X-Y (Fig. 1), after Schwebel! showing Flinders University stratigraphic borehole und

AMINO ACID DATING OF LATE QUATERNARY STRANDLINES

samples beyond the range of ™C techniques

(Schwebel 1979)",

Saniple localities

Maternal used for AAR dating was obtained

from localities A, B and C (Fig. 2) on the

transect X-Y (Pig, 1), ‘The molluse Katelysta

yedlurina, (Lamarck) waa selected as the

gpecies most suitable for the raccinzation

analysis since it has relatively thick. nen-

porous. vailves,

Sample A is a surface sample from a shallow

pit at Lake St Clair where articulated speci-

mens were selected, This locality lies on the

first interdune flat inland from the present

coast, where dates ou molluscs have been

reported by Blackbur (1966) at 4330 = 100

years using MC. Stratigraphic observations hy

Schwebel (1979) are in accord with the above

date, and show the sediments to have been

deposited during the peak of the Holocene

sealevel transgression prior to final separation

of the Mat from the ocean by modern barrier

accretion and possible sea level decline. Be-

cause of the established radiocarbon dates, this

sample was used us a reference point far the

calculations involved in determining the ages

of samples Band C.

Sample B ig from the side of a dram locally

known as Drain L which interseets the Woak-

wine Range harrier and ils related estuarine-

lagoonal strata to the east, Shells comprising

sample B, many of which are in-situ, occur

withm a 20-30 em thick indurated layer, on

an erosion surface which is onlupped by Holo-

cene Jucustrine calcareous muds of the mast

recent lake Hawdon phase.

Sample C. interpreted by Schwebel (1979)!

to come from the same horizon as that of

sample B, was collected fram a stratigraphic

horchole (Fig, 2) from a molluse-rich layer

280 em below the sediment surface. Articulated

samples of Kavelysia sealarina (Lamarek)

were sampled and used for dating,

Dating methods and procedures

Approximately 5-10 grams of a single

eleaned Katelysia valve were processed accord-

ing to the procedures desenbed for the “total”

fraction by Masters & Bada (1977). The

alloigoleucine/isoleueine (alleu/iso) ratio was

determmed on a Beckutun-Spinco Model 118

__ Sa rrrrovr'"—

7 Schwebel, DA. (1979) Quaternary stratigraphy

of the southenst of Soulh Australia. PhD.

thesis (unpubl). Flinders Univ. of S, Aust.

has

TanLe J. Baten of siting avid pacemeiation ty

iKarelysin shelly fren mranite terrace depestta dry

angrherne otistraliy

vt glutumie Del alleu!

Sample alanine = acid ~—s leucine isa

A 0.29 O17 028 O11

B DA 0.30 O35 028

Cc O73 N37 O46 036

Modern Katelysia 0,13 0.08 O09 0.01

automatic amina acid analyzer, The enantio-

meric ratios of ihe other amino acids were

determined by gas chromatography of the

N-Irilluaroacetyl-L-prolyl peptide methyl esters

(Hoopes et al. 1978).

Results and discussion

The racemization results for the various

samples are given in Table 1. The extent of

AAR in sample A ts consistent with a Holo-

cene age for this sample, Substututiag the

measured alleu/iso ratio and an age of 4330

years (Blackburn 1966) in eq. (2) of Mas-

ters & Bada (1977) yields k,, = 2.3 * 10%

yori. The value of K,,, in this equation was

assumed to be ~1 3, This kj, value is in close

agreement with that calculated using Holocene

Chiene molluscs from Southern California

coastal archacological sites, This is the expected

resull due to the similarity of the mean annual

cir temperatures of the Califarman and South

Australian localities (Felton 1965: Floegel

1972). and since the Katelysia and Chione

species have similar shell morphologies.

idendeal to that measured in Chinne (Masters

& Bada 1977) and Pretathaca molluses (Weh-

miller 1977) from a terrace deposit in San

Dicyo, California. This terrace has been dated

al 120000 = |G000 years by vranium-serics

uating of corals (Ku & Kern 1974). Since the

Holocene saniple suggests that the rate of

racemization is similar at the Californian and

Australian sites, the sinvlariny of the extent

of racemization in sample C and the 120 :000-

year-old Californian terrace supports the con-

clusion that sample C corresponds in age to the

maximum high-sea level stand dunng the last

interglacial period (ic. Stage 5e in the 04/01

palacotemperature curve, ~125 000 B,P,).

In comparison ta sample C, the extent of

AAR is consistently slightly less in sample B.

On this basis, fi would appear thal sample B

may come from one of the other episades of

170 C. C. von der BORCH, J. L. BADA & D. L. SCHWEBEL

high sea level, tentatively dated at ~85 000

and 105000 years B.P., which occurred in

the vicinity of the last interglacial period

(Bloom et al. 1974). Substituting the measured

alleu/iso ratio for sample C and an age of

120 000 years for this sample into eq. (2) in

Masters & Bada (1977), yields Kis. = 2.9 X

10-"yr-". Using this ki,» value to date sample

B yields an age of ~92 000 years.

The AAR dates for samples B and C given

above imply that the uppermost portion of the

Woakwine Range strandline complex was

formed during the last interglacial high sea

level. This is in accord with the uranium series

data of Schwebel (1979).

Sample B with an age of 92000 years

appears slightly younger than C, which is about

120 000 years old. In fact, the age of B lies

approximately midway between the 85 000

and 105 000-year-old sealevel highs described

by Bloom ef al. (1974). If the assumption is

made that C actually correlates with the

125 000 year sealevel high (i.e. that the date

used to calculate the k;,,, value given above is

a few thousand years too young), then B could

possibly be correlated with the established

105 000-year-old sealevel high. On the other

hand the small number of samples, and the

resolution of the amino acid dating technique

as applied to the study area, may imply only

that the two samples B and C were laid down

in response to some stage or stages of the last

interglacial sealevel maxima, of the order of

120 000 years ago.

Acknowledgments

We thank D. Darling and E. Hoopes for

assistance with the racemization analyses. The

racemization work was partly supported by a

grant from the U.S. National Science Founda-

tion (Grant EAR 77-14490). Manuscript

typing was done by Nena Bierbaum and

diagrams were drafted by Gail Jackson.

References

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——. Bonn, R. D. & Crarke, A. R. P. (1967)

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BLoom, A. L., BROECKER, W. S., CHAPPEL, J.,

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Cook, P. J., Cotwetr, J. B., Firman, J. B.,

LinpsAy, J. M., SCHWEBEL, D. A. & VON DER

Borcu, C. C. (1977) The late Cainozoic sequence

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Geophys... 2, 81-88.

Fetton, E. L. (1965) “California’s many

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Fiorcer, H. (1972) The position of the lower

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Universitat, Miinchen.

Hays, J. D., Imprie, J. & SHACKLETON, N. J.

(1976) Variations in the earth’s orbit: Pace-

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Hitts, E. S. (1960) “The physiography of

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Hoopes, E. A., PeLTzer, E. T. & Bana, J. L.

(1978) Determination of amino acid enantio-

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the N-trifluoroacetyl-L-prolyl-peptide methyl

esters. J. Chromat. Sci. 16, 556-560.

HossFetp, P. §, (1950) The late Cainozoic

history of the southeast of South Australia.

Trans. R. Soc, S. Aust. 73, 232-279.

Ku, T. L. & Kern, J. P. (1974) Uranium-series

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San Diego, California. Geol. Soc. Amer. Bull.

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Masrers, P. M. & Baba, J. L. (1977) Racemiza-

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ete ae Earth and Planet. Sci. Lett. 37,

73-183,

—— (1978) Amino acid racemization dating of

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SHACKELTON, N. J. & Oppyke, N. D. (1976)

Oxygen isotope and paleomagnetic stratigraphy

of Pacific core V28-239 late Pliocene to latest

Pleistocene. Geol. Soc. Amer. Mem. 145, 449-

464,

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east province, South Australia, with special

reference to Quaternary coast-line migrations

and modern beach developments. Bull. Geol.

Surv. S. Aust. 29,

VON DER Borcu, C. C. (1976) Stratigraphy and

formation of Holocene dolomitic carbonate

deposits of the Coorong area, South Australia.

J. sedim. Petrol. 46, 952-966.

WEHMILLER, J. F. (1977) Amino acid studies of

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Lett. 37, 184-196,

NEW CRETACEOUS AND TERTIARY CRABS (CRUSTACEA:

BRACHYURA) FROM AUSTRALIA AND NEW ZEALAND

BY §. BARKER

Summary

From the Cretaceous of Australia and New Zealand three new genera of Brachyura, one new

subgenus, and seven new species are described and one new family is proposed. Four new species

from the Eocene are described, one from Australia and three from New Zealand, and changes in

taxonomy and nomenclature are made. The new classification of the Brachyura (Guinot 1977) is

applicable to the new material which contributes significantly to the clarification of taxonomic and

phylogenetic relations at an early, critical stage in the evolution of the Brachyura. Modified Tethyan

palaeobiogeographic relations of the Cretaceous and Palaeogene faunas are recognised.

NEW CRETACEOUS AND TERTIARY CRABS (CRUSTACEA: BRACHYURA)

FROM AUSTRALIA AND NEW ZEALAND

by M, F. GLAgSSNER™

Summary

GLAgssNER, M, F, (1980) New Cretaceous and Tertlary crabs (Crustacea, Brachyura) from

Australia and New Zealand, Trins. 8. Soc. 8. Aust. 104(6), 171-192, 24 November, 1980.

From (he Cretaceous of Australia und New Zealand three new genera of Brachyura, one

few subgenus, und seven new species are described and one new family ts proposed. Four new

species from the Bocene are described, one from Australia and three fram New Zealand, and

changes in taxonomy and nomenclature are made, The new classification of the Brachyura

(Guinet 1977) is applicable to the new material which contributes significantly to the clan

ficalion of taxonomic und phylogenetic relations at an early, crilical stage an the evolution of

the Brachyura, Modified Tethyan palacabiogeographic relations of the Cretaceous und Paluea-

gene faunas ure recognised.

Classifivation

A new classification of the Decapoda

Brachyura praposed by Guinot (1977, 1978)

is of particular interest to students of the

evolution of these ¢éruistaceans, Based on

generally sound and stated principles, and on

a re-examination of a very large amount of

zoological material as well as literature, it

takes into consideration conclusions Treached

hy palacontologists, questioning some of these

conclusions specifically. New material from

Australia and New. Zealand provides a suitable

starting point for the task of answering some

of the queries raised, and of testing the

suitability of the proposed new system of the

Decapoda Brachyura, The following tabulation

places the ncw finds in the framework of

Guinot’s classtfication and indicates their age

and oceurrence.

Section Podotremata Guinot, 1977

Subsection Dromiacea de Haan, 1533

Superfamily Homolodromioidea Alcock, 1899

Family Prosopidac von Meyer, 1860

Oanoton woodsi nov, gen,, nov. sp. Upper

Albian, central Queensland and South

Australia.

Subsection Archaeobrachyura Guinot, 1977

Superfamily Homoloidea White, 1847

Family Homolidae White, 1847

Heamelapsis etheridee? (H. Woodward, 1892).

Upper Albian, central Queensland.

Homolopsis spinulosa nov. sp. Upper Ceno-

mianian, northern Australia.

= Department of Geology, University of Adelaide,

Box 498 G.P.O,, Adelaide, 5. Aust, 5001.

Superfarmly Raninoidea de Haan, 1833

Family Raninidae de Haan, 1833

Notepocorystes (Cretacoranina) exiguus Twv,

sp, Lower Cenomanian, Northern Australla,

Hemioon nevezelandicum nov. sp. Upper

Albian, New Zealand.

Ranilia porerariensis nov. sp. Upper Bocene,

New Zealand.

Lyreidus waitakiensis nov, sp. Middle to Upper

Eocene, New Zealand.

Superfamily Tymoloidea Alcock, 1896,

Family Torynommidae nov, fam,

Torynomma (Torynomma) flemingi nov. sp.

Upper Senonian, New Zealand,

Torynomma (Paratarynamma) dentatyim nav,

subgen., nov. sp. Upper Cenomanian—

Lower Turonian, northern Australia.

Diorationus salebroxsus Woods, 1953 Upper

Albian, Queensland and South Australra.

Dioratiopus sp. Upper Cenomanian, northern

Australia,

Eodorippe spedeni nov, gen., Noy. sp. Upper

Senonian, New Zealand.

Section Heterotremata Guinot, 1977,

Superfamily Portunoidae Rafinesque, 1815

Family Portunidae Dana, 1852.

Subfamily Psammocarcininae Beurlen, 1930.

Rhachiovoma granalifera (Glaessner, 1960)

Upper Eocene, New Zealand.

Family uncertain.

Pororaria eocenica noy. gen, nov. sp. Upper

Eocene, New Zealand.

Superfamily Xanthoidea McLeay. 1838,

Family Panopeidae Ortmann, 1893.

Panopeus whittenensts nav. sp, Upper Eocene,

South Australia.

The most distinctive innovation alfecting ihe

classification of the Brachyura discussed here

172

is the demotion of the “Section Dromiacea”

which has dominated considerations on the

origin and evolution of the Mesozoic Brach-

yura for more than a century. Guinot recog-

nises three sections: the Podotremata, Hetero-

tremata and Thoracotremata, named accord-

ing to the position of the gonopores, This looks

rather like a single-character classification to

which I objected (Glaessner 1969) when the

peditreme-sternitreme distinction (Bouvier

1897) was used by Gordon (1963) to remove

the former group from the Brachyura. How-

ever, Guinot (1978) has amply demonstrated

that it is a distinction by grades, the use of

which she finds inevitable for taxa of high

rank while following to some extent “pré-

occupations d’ordre cladistique” for lower-rank

taxa. This taxonomic innovation involves

recognition of two subsections of the Podotre-

mata, the Dromiacea and the Archaeobrach-

yura. The former comprise the Superfamilies

Homolodromioidea and Dromioidea, the latter

the Homoloidea, Raninoidea and Tymoloidea.

This classification is significant for the present

investigation. There is ample morphological

evidence for close links between the Tymo-

loidea and the Homoloidea, The Dromioidea

(Families Dromiidae and Dynomenidae) have

taken a different evolutionary path. With

reference to the descriptions and discussions

which follow, it is sufficient to note here that

Homolopsis and Torynomma (with related

genera) are morphologically close and, as

Wright & Collins (1972) have indicated,

appear to have had Prosopidae, hence Homo-

lodromioidea, as ancestors in Jurassic time.

The Dromioidea differ significantly from this

group in many morphological, embryological

and ethological characters. For the question

of the evolution and systematic position of the

Raninoidea there is no significant new material

under discussion here (see Forster 1968,

Stevcié 1973). I had previously (Glaessner

1969) assigned the Tymolinae to the Dorip-

pidae, following the latest comprehensive clas-

sification available at that time (Balss 1957).

This is now unnecessary and unacceptable,

since Guinot’s work has shown that the oxy-

stomatous condition (which has to do with the

direction of the inhalent and exhalent currents

of water under the carapace) was reached

independently by very different groups of

crabs. Thus there is no justification for

retaining the artificial taxon Oxystomata.

With this demonstration most of the major

classification of the Brachyura, of long stand-

M. F. GLAESSNER

ing but often questioned, had to be abandoned.

The origin of all or some of the older Hetero-

tremata (Dorippoidea, Calappoidea, Cory-

stoidea (+Cancriformia), Portunoidea and

(questionably) Xanthoidea (see Wright &

Collins 1972) from Cretaceous Tymoloidea or

their ancestors is possible or even probable,

but these investigations would lead beyond the

limits set by the material here described.

Summary of stratigraphic distribution

(New Zealand species marked with asterisk)

Upper Albian: Oonoton woodsi, Homolopsis

etheridgei, *Hemioon novozelandicum, Diora-

tiopus salebrosus,

Lower Cenomanian: Notopocorystes (Creta-

coranina) exiguus,

Upper Cenomanian: Homolopsis spinulosa, D.

sp.

Upper Cenomanian to Lower Turonian: Tory-

nomma (Paratorynomma) dentatum.

Campanian-Maastrichtian: *Torynomma (T.)

flemingi, *Eodorippe spedeni.

Middle to Upper Eocene: *“Lyreidus waita-

kiensis.

Upper Eocene: *Ranilia pororariensis, *Rha-

chiosoma granulifera, *Pororaria eocenia,

Panopeus whittenensis.

Remarks on palaeobiogeography

While we know only a small sample of the

Brachyura of the Cretaceous and Eocene of

Australia and New Zealand, theoretical con-

clusions are unwarranted. It is worth noting

that known relations are dominantly with

European genera. Homolopsis, Notopoco-

rystes (which is almost cosmopolitan),

Hemioon, Dioratiopus, Rhachiosoma and

Panopeus (which is also Atlantic) are well

known from Europe. As far as the Austra-

lasian region is concerned, the origin of these

genera can be considered as Tethyan. Tory-

nomma has its range extended from Queens-

land to the north of Australia in the

Cenomanian, and to New Zealand in the

Campanian-Maastrichtian. Its close relative

Dioratiopus, a genus shown to include many

European species, is recorded, in addition to

Queensland, from northern South Australia

and from Melville Island north of Darwin.

The undescribed macruran and thalassinacean

decapods from the Cenomanian of the island

(Paraclytia, Hoploparia, Trachysoma and

Protocallianassa) are well known from the

European Upper Cretaceous. The Tethyan

NEW CRETACEOUS AND TERTIARY CR VBS

relations of the Brachyura from Bathurst

Ishind are in agreement with Lhe character of

its Cenemanian ammonue fauga (Weight

1963), Eodorippe trom the Upper Senenian of

New Zealand is endemic, and the endemic

Recent. Nectocarcinuy may have had an ances-

tor dating back to the Eacene in the same

region, the new genus Porotarta.

Descriptions

Family Prosopidae

Oonotim nov, gen,

Derivation of name: From Greek oon:

eee, noton; back, with reference to shape.

Diagnosis: Carapace ovoid, without sharp

lateral margins, posterior margin short, ros-

trum triangular, truneated, with transverse

groove and row of graniiles at bases eye sockets

close-set with strong supra- and infraorbital

spines; mesogustrie lohe long and narrew.

uragastric lobe indistinct, carapace surface

granulated,

Thad intended to assign this fossil to Fectls

Withers, 1946, but Mr C. W. Wright kindly

informed me in July 1980 of his disagreement

with such an extension af this taxon, | accept

his view that the differenees between the

Australian ¢fab and the three English species

ure of generic significance, They leave Gono-

ton closer to Veerlsy than to other genera,

Oonoto woodsi nov, sp.

Derivation ef names After Dr J, T, Woods,

Director of Mines, Queensland who has made

Valuable contributions to the knowledge of

Cretaceous Decapoda from Queensland,

Material: 1. Holotype—An almost complete

carapace. Qld Mus, K 2876. 2. One ffag-

mentary carapace, Geological Survey of

South Australia No, Cr 1.

Localities: 1. Currane Station, 16 ki N of

Dartmouth, central Queensland. 2. 14 kin W

of Mt Dutton (Loe, 17, Miap Sheet 5/571,

see Bull 40, Geol, Survey S. Aust. p. dd).

Preservation; The Queensland specimen is

well preserved in a smooth, round, concre-

tionary nodule, similar to those which contain

other crabs from the Queensland Cretceous,

The South Australian specimen consists of

internal moulds of two angular fragments of

the posterior portion of the carapace, partly

overlapping, in a concretion containing

numerous mollusea, The mode of preservation

and the assactalion suggest that the carapace

may have been broken hy a predator, probably

a belemiite or an anymenite

173

Ages Upper Albian, Tambo Formarion of

Queensland and Oodnpadatta Formation ot

South Australia,

Descripiun: Curapace of holotype avoid,

27 mm long, 224 mm wide, about 8.5 mm

high Convex antero- aid posterolaceral mar-

gins of ahoul equal length; lateral margins

almost parallel, longitndinal and transverse

profiles of carapace (Pigs, 1A, B) strongly

and smoothly convex. Apically truncated

triangular rosttul plate directed forward, set

off from (interior slope of curapave by trans-

Verse groove afd row of granules in front of

mesovastric region. Eye sockets deep and

small, with strong, conical, supraorbital and

long infraorbital spines Which are twice as

long and set helow. Anteralateral outlines

diverge 10 crossing points of cervical grooves

and widen only slightly to metubranchial

regions. Posterior margin apparently not as

long as in Vectly, Regions well marked by

smooth, shallow furrows. Mesogastric lobe

not subdivided, Almost entire surface of cara-

pave fairly evenly covered with large granules

Additional small tubercles on metabranchial

regions, and 5 distinctive, lurger, granulate

elevations. Two are symmetrically arranged

on mesogastric lobe, 2 of metragastric lobe

which is divided by deep median furrow, |

on cardiac lobe, sy distance from posterior

margin 4 that from hase of rostrum, Cardiac

erades into narrow intestinal lobe,

This species differs from two Aptian and

nne Albian species of Vectiv previously des-

cribed from Envland in details of shape and

surface sculpture, Tt has all the significant

characters of their carapace regions but they

ure uot as tum and therefore less con-

spicuous in the new species, The characters

which are preserved in the smaller specimen

from South Australia do not differ from those

af the holotype from Queensland,

Family Homolidae

MHomalopyis Bell, 1863

Homolopsis etheriduct (Woodward. 1892)

FIG. 2

Presapon elleridee’ Woodward 1892, p, 301, pl

4) Erhevidge 1917. po 5, pl 1, fix, 1-4,

Harmolopyiy etheridgels Vian Sraelen, 1928, p, 6195

Woods, 1953, p, 30, pl. 2, fig, 1-3, text fig 1.

Material: One almost complete specimen

(P22945),

Lacality: “Currane’, 14 km WN of Dart-

mouth. central Queensland, Coll, J, T, Woods

1955.

SSNER

, Bo a

NEW CRETACEOUS AND TERTIARY CRABS \72

Aye: Upper Alan, Tambo Formation.

Remarks: This specimen is figured here for

comparison for completeness of the record of

currently known Australian Cretaceous crabs,

ft hus a significantly more convex carapace

than the species figured by Wright & Collins

(1972) and its Upper surface ws certainly not

“mare or less flat” as their generic diagnosis of

Haomolopyis requires, Tt may be appropriate

to place the Australian species in a new sub-

genus unless species with traditional shape

Characters exist.

Homplopsis spinulosa nov. sp.

FIG. 3, 3A

Holotype material: Once small, somewhat

crushed specimen with counterpart, P22934.

Coll. B. Daily 1954

Locality: South coast of Melville Esland,

N-f., about 10 km NW of Cape Gambier.

Ave: Upper Cenomanian, Bathurst Island

Formation, about 8 m above “Tapara Bed"

Preservation: Preserved in a slightly

weathered yellowish clay is the cepbalothorax

with two abdominal somites, the left cheliped

and parts of all other perciopods. Ferruginised

and affected by compaction and weathering;

most of the carapace margins defective. Arti-

ficial moulds of the counterpart show details

fot recognisable in the damaged specimen,

Description; Carapace about }2 mm tong

and td om wide, fronto-ocbital width about

8 mm} anterolateral margins diverging, Pos-

(erolateral margins slightly converging;

posterior margin about 5 mm long, curved,

with granulated edge, Ornamentation consists

of distinct, granulated tubercles; at least |

epigastric, 2 protogastric, | hepatic, 2 ept-

branchial and 3 metabranchial tubercles

present on each side and also metagastric and

cardiae tubercle-bearing ridves. Surface finely

and evenly eranulated. Left cheliped short and

robust, with a spindse carpus; P2 and F3

strong. long, with spinose edges, the P4 appear

near the posterolateral angles of the carapace,

thin, smooth P5 near the hase of the abdomen,

First two abdominal somins about 5 num wie,

rectangular in outline, subequal, about 0,75

ne Eee E EEE SenS Sn

grooves and cleyations on a blunt transverse

ridge on gach somite, Abdomen extending

horizontally backward.

This species appears to differ from other

species of Momolopsiy and also from “Glaess-

nerie” depressa (Carter) as described by

Wright & Collins ((972) mainly in details of

ornamentation, The linea homolica ts partly

visible and partly obscured by conipression and

fracturing of the only known carapace,

Family Raninidae

Notopacorystes NVCoy, 1849

Natopocorystes (Cretacoranina) exiguus

nov, sp.

FIG, 4, 4A

Derivation of name: From Latin exiguus;

small,

Material: One carapace, with counterpart,

in w bore core. Forwarded by Mr PF. Bollen,

P22929,

Locality’ Bathurst Island Ojl| Development

Well No. 2, about 4 km N of the mouth of

Pipanyamilr Creek, about 30 km W_ of

Bathurst Island Mission, Care from 280 m

depth,

Age: Lower Cenomanian, Bathurst Island

Formation, grey clay.

Preservation: Carapace undistarted but most

of the extremely fragile shell attached to the

counterpart and anterolateral and orbital mar-

gins damaged.

Description: Carapace ovoid, 15 mm long,

10 mm wide. Width of the fronto-orbital

margin about 5.4 mm, Carapace gently convex

transversely and longitudinally, greatest height

in the centre. Median ridge very faint. Rostrum

hifid, medially grooved, slightly detlexed. Two

supruorhital fissures. Extraorbital teeth could

riot have been large. Orly a very weak lateral

tubercles, 1 hepatic, | cpibranchial and 1

extremely weak mesobranchial, followed by a

finely granulated ridge along posterolateral

margin. Posterior margin about 6 mm long

but not well preserved. Cervical furrow, gently

curved, runs from a notch in front of the epi-

branchial luberele in a forwardly convex curve,

then follows @ sinuous course to distinct pos-

terior gastric pits. Epibranchial turrows short,

mm Jong. with two longitudingl shallow

Pig. |. Qanoren waedst nev. sp. x2.

Fie, 2. Momolopsiy ethertitge’ (A, Woodward).

Fig. 3. Mamolapsis sninulasus nov. sp, x3,

fie. 4. Netopocorysies (Cretacoranina) extyvuy nay. sp. x3.

Fig. 4. Memioen nevoselandicun nov. sp, x3.

Pip. 4. 6a. Ranilia porerariensis nay, sp. x2, a—dorsal view, b—ventt wl view

176

10mm

10 mm

M. F. GLAESSNER

10mm

10 mm

NEW CRETACEOUS AND TERFIARY CRABS 7

iransverse, do not reach the cervical groove.

Branchiocardiac furrows more distinct, particu-

larly their posterior edges, merging with the

deep epimeral grooves. Epimeral and posterior

gastric. muselé attachments well marked on

ihe inside of the carapace, The described Cur-

rows, together with hepatic and Weaker

Mesogastric furrows form # peculiar radiating

pattern on the outer surface which Is finely

pitted and granulated, Two elongate, tubercu-

late protuberances on the anterolateral parts

of the carapace: outer ones smaller .and

prominent on the fepalic lobes, inner ones

situated on outer portions of the protogastric

lobes Which are partly separated from the main

paris by shallow grooves,

Remarks: The weak marginal spines and the

surface sculpture plave this species in the sub-

genus Cretacoranifa Mertin, 1941, It does not

appear to he particularly close to any of its

known species but detailed coniparison must

await the discovery of further specimens.

Hemioon Bell, 1863

Hemloon novezelandioum mov, sp.

FIG. 5, SA

Holotype material. Gne specimen in a hurd

conerction. Geologival Survey of New Zeuland

GSI 1845,

Loealiry: Swale Stream, Coverham, South

Island of New Zealand (P30/f 36}.

Age: Latest Albian, Lower part of Swale

Siltstone, Ngaterian locul Stage, Dr |, Speden

(in fitt, 1977) suggests lower Ngateriau, from

near the base of the Worthuceray parvum

Assemblage Zone of Henderson (1973).

Preservation; Cephalothorax preserved as an

internal mould, eff central position, in a Very

hard concretion which does not split evenly.

Sternum not visible hut fragments of Jegs und

chelae preserved im slightly displaced positions

and much of the inside of the carapace shell is

visible. Although the rostrum remained th

the Counterpart matrix when the coneretion

was split, it was possible to extruct its tip and

rejoin it so that the length of the rostrum could

he determined (Fig, SA).

Peseription: Cephalothorax ovoid, flattened

jonwitudivally and convex, transversely, lateral

margin discontiniious, weakly developed, ‘Two

weak anterolateral spines aml un acicular

extraorbital sping with yranulated surface.

Orbits large, well marked, with two supra-

orbital fissures and a stout supraorbital tooth.

Rostrum about 3 mm long, straight, with two

jateral basal spines. Markings on carapace sur-

face very weak, Internal mould shows median

parts of cervieal groove curving laterally from

posterior gastric pits, the anterior tip of the

Mesagasinc lobe, epimeral grooves, and relics

of the ‘branchiocardiac grooves, Narrow

median ridge marking cardiac und mlestinal

lobes, Strong muscle pits in the hepatie regions.

Surface of carapace finely pitted where it can

be seen, Posterolateral margins granulate, The

greatest width (16.5 mm) is found hetween

postermlateral (marging Which are separated

trom the anterolateral margins by a slight

constriction behind the second anterolateral

teeth, Marked, nirrow, pterygostomial ridge

and a wide depression alone brachiostegite.

Posterior margin missing. Carapace was al least

25 mim long, greatest width is ac about 0.6 of

its length.

Remarks: The new species differs from A,

clangatvin (A. Milne Edwards 1862) in the

shape of the carapace, the weak lateral tecth

und the absence of surface tubercles, A, etr-

cvmniatay Wright and Collins 1972 also has

strung unterolateral spines and convergent

lateral margins on the posterior half of the

carapace. These differences remove the new

spevics further from Raninella ws revised by

Wright & Collins than those eansidered by

these authors {t differs more in shape and

carupace sculpture from Netopacarystes (Cre-

facoranina),

Raailia H, Milne Edwards, 1837

Ranilia pororariensis noy. sp,

PUG, 6, 6a

Helorype eaterianl One carapace. slightly

Uistortect by flattening, most of Fronto-orbital

margin missing, Chelipeds and some displaced

oy broken pereciopods preserved, sternum not

Fin 1A. Danoten woadst nov, sp.. left side view: IB front view. SO—position of supreurbital spine,

To-infraorbital spine. Stippled parts of campate are missing or concealed.

Fig. 3A. Hemvlopsis spinulosus Nov, so. Partial reconstruction Dotted line indicates outline of erushed

caramice,

Vig. 4A. Netopocoryaiey (Creiacorunina) exigins poy, sp. Reconstruction of carapace showing pattern

us scen on inner surliee.

Fig. SA. Henioon novezelancdiedia ney. sp. Reconstruction of carapace. Stippled paris are missing

Fig. (2A, Diorwiopus solebrasis Woods, Reconstruction of carapace.

Fig, I3A. Epdorippe speden? oov, sp, Diagrammatic recanstriction of carapace pattern and rostrum.

178

visible, first abdorainul somite preserved, Can-

terbury Museum, Christchurch, New Zealand,

No.zfe 7, Coll, RK. S, Allen, Feb. 1935.

Localirys Coastal cliffs at Pororari, 2.4 km

N of Punakaikt. Sheet No, $37/723, Grid ref.

C852318.

Age; Kaiatan—Runangap, Late Eocene.

Description: Carapace ovoid, strongly con-

vex transversely; height about equal to half

the width; gently convex longitudinally

Distance between the extraorbital and lateral

acicular teeth equals that between Jateral teeth

and point of greatest width which is at the

level of the posterogastric pits; distance from

this point to posterior margin almost 3

times longer, Posteriorly convergent postcro-

lateral margins marked by a smooth ridge

which is convex in dorsal view for first half of

their length, then straight, Posterior margin

straight, A very faint median ridge on posterior

half of carapace, Two supraorbital fissures

separated by ~ small tooth, only base preserved,

Surface of carapace uniformly pitted, marked

only by weak epimeral muscle impressions.

First abdominal segment trapezoidal, surface

pitted but otherwise smooth. Propodus of

cheliped has sharp, denticulated upper edge

and strongly deflexed fixed finger, Dactylus

gently curved, with narrow dorsal groove

hetween two ridges,

Remarks; The new species differs m shape

and ornamentation and in the deflexed fixed

finger from living species, [t is distinguished

by the weak longitudinal ridge and the antero-

lateral teeth from the Eocene R, (“\Noatopella”)

vareolata (Lorenthey), Further specimens in a

better state of preservation and preparation are

required for complete description and com-

parison,

Lyreidus de Haan 184

Lyreidus waitakiensis nov. sp.

FIG. 7, 7a

Halotype material? One carapace, front

mostly missing, Canterbury Museum, Clirist-

ehureh, New Zealand, No. zfe 30,

Loculity: Black Point, Waitaki Valley.

§127/368, Grid reference c 364 916. Another

less well preserved specimen (Canterbury

M. FF. GLAPSSNBR

Museum, No, 2fe 8, coll. R. S. Allen Feb,

1935, frotn coastal cliffs at Pororari, 2.4 km

N of Punakaiki) probably belongs to this

species.

Age; Middle to Upper Eocene, Tapui glau-

conitic sandstone, Bortonian Stage. This may

he the oldest kiownh species ef Lyreidus. The

Other specimen, tentatively mamed L. ef-

waltukiensis, is from the Upper Evcene,

Katatan-Runangin.

Preservation; Inner layer and parts of outer

ol shell of holotype present. Complete

branchiostegites, part of the left antennal base

and smull, displaced sternal fragments also

preserved,

Description: Carapave ovate; Pronto-orbital

region 6,5 mm wide, with 2 supraorbital fis-

sures; anterolateral margins diverging from the

extfaorbilal ta obliquely pointed lateral tecth.

Distance between their tips is about 3,5 nim,

equal to greatest width of carapace measured

about 3 mm behind them, Abterolateral mar-

Bins tounded, uv bluntly conical tooth on each

side halfway between extraorhital ynd laceral

teeth, A blunt edge extends a short distance

behind the lateral teeth, replaced Irom below

by a distinct, sharp, posterolateral ridge with

amall granules. Posterolateral margins con-

verge 10 afelale posteriie margin which

equals fronta-orbilal margin in length, Cara.

pace strongly convex transversely, gently con-

vex Jonvitudinally, pterygostomial regions

inflated. Pleural suture sinuous anteriorly.

parallel fo lateral margits and a shore distance

below then, Surfice of carapace shows pose

terogastric pits 2 mm behind tevel of the

lateral teeth, und weak epimeral stiractor

muscle markings sume distanee behind them:

smooth hut may have beet faintly pitted and

weakly granulated jf) some places, Two weak

epigastric yuhercles. Pterygostomial regions

aranwilated. Orbits only slightly oblique in

frontal, view. witht small infraorbital spines

separaled by fissures from extraohital weth

Anteunal base has taleral, longitudinal, eranu-

lated mupe with channel along its cuter side,

helween it and edge of carapace; jt may lead

tn the proximal side of the infraorbital tooth.

Remarks: This species can be distinyulshed

by its avoid shape and its ornamentation, ‘Che

ee eeSFSFSSSSSSSSSSSSSSSSSSSS——eaieseseseseFh

Fig. 7, 7a, Lweidnus woinekiensis nov. sp. x2. a—dursul view, b—ventral View,

Fig. & Toryronima guadratum Woods. Plaster cast of holotype, x2. Rostrum drawn from anuther spe-

cimer.

Figs. 10, 11, Tarvnammea (Paroterynemmad) dentetum ney sp

')—holoryye. “15, dersal view. Tp

Paratype P2231. x2. Ventral view with atener stermum and abdumen of 9 sind perciopaids.

NEW CRETACEOUS AND TERTIARY CRABS 179

180

shape of the carapace appears to be of slightly

more generalised raninid type than in the

Miocene and living species which are

anteriorly more sharply narrowed and strongly

elongated,

Family Torynommidae nov. fam,

The genus Torynomma was originally placed

in the family “Prosoponidae” (recte Prosopi-

dae), together with Dioratiopus (Woods 1953,

p. 52). These genera have hardly more than a

few primitive (plesiomorphic) characters in

common with the Prosopidae but they do not

have any of the distinctive, diverse develop-

ments of shape of the carapace and rostrum

or the dominance of the transverse carapace

grooves which characterise this family. The

placing of Torynomma, Dioratiopus and other

extinct genera in the subfamily Tymolinae

Alcock, 1896, as proposed by Glaessner

(1969) is considered inappropriate by Wright

& Collins (1972). Concerning the placing of

the Tymolinae in the Dorippidae, Gordon

(1963, p.56) stated: “Certainly the so-called

Tymolinae with sternal furrows and coxal

genital pores should not be placed in the same

family as the dorippids without sternal furrows

and with the genital openings of the female

sternal”. I rejected (Glaessner 1969, p.R440)

Gordon’s further conclusion that it seems

logical to exclude all peditreme crabs “from

the Brachyura, restricting the term to the vast

majority of crabs with the female genital

openings sternal’. I noted that the Dromiacea,

Raninidae and Tymolinea which have coxal

female gonopores are “exceptional” and that

their separation “on the basis of an obviously

primitive character is an extreme application

of ‘horizontal classification’ which is not

acceptable, particularly as the steps in the

evolution from the primitive peditreme to the

advanced sternitreme condition have not yet

been studied on fossil material”. Hence I fol-

lowed the earlier systematists and Balss (1957)

who placed the Tymolinae in the family

Dorippidae. Guinot’s work (1977, 1978) has

now removed the traditional major subdivi-

sions of the Brachyura such as the Oxystomata,

which had been hampering the development

of systematics in this group since the middle

of the last century. It showed that Gordon

had been remarkably far-sighted in recognising

the peditreme-sternitreme evolutionary transi-

tion as a fundamental change which can

provide a firmer basis for the major classifi-

cation of the Brachyura than the diagnostic

characters of the traditional major taxa, How-

M. F. GLAESSNER

ever, this reclassification also rejected Gordon's

“logical conclusion” that the peditreme crabs

are not Brachyura. The steps in the evolution

from the peditreme to the sternitreme grade

(Guinot’s Sections Podotremata and Hetero-

tremata) are now better documented both in

living and in fossil forms including those

described or reconsidered here. Earlier

erroneous classifications on family and sub-

family level (Balss, Glaessner) must now be

corrected in the light of these data. However,

they are still incomplete as far as palaeonto-

logical material is concerned,

Wright & Collins (1972) assigned to the

family Cymonomidae (erroneously ascribed

to Ihle 1916 but actually named by Bouvier

1897 as Cymonomae) the fossil genera

Glaessneria Wright & Collins, 1972 (re-named

Glaessnerella in 1975) and Dioratiopus J. T.

Woods, 1953, considering them as “closely

allied”. Tt will be shown below that they are

synonymous. Also included was Mithracites

Gould, 1859, but Withersella Wright & Collins,

1972 and Binkhorstia Noetling, 1881 were

omitted and rather unconvincingly placed in

the Carcineretidae. The fossil genera included

by Wright & Collins range from Lower Aptian

to Cenomanian; Binkhorstia is Maastrichtian.

I have included in the subfamily Tymolinae

the Upper Eocene Falconoplax Van Straelen,

1933. Its sternum is flat and wide, with a deep

abdominal depression and well marked sternal

grooves between sternites 4-8 and a deep

furrow in the anterior portion of sternite 8 of

the female. On the criteria used by Guinot

for suprageneric taxa it would seem necessary

to exclude this genus. The Tymoloidea, accord-

ing to Guinot (1978) with one family Tymo-

lidae, comprise 2 subfamilies Tymolinae

Alcock, 1896 and Cymonominae Bouvier,

1897, in which the living genera Cymopolus

A. Milne Edwards, 1880 and Cymonomus A.

Milne Edwards, 1880 are included, They have

a square, rugose, granulate or spinose cara-

pace, a narrow, triangular, pointed rostrum,

reduced eyes or fixed eyestalks without

cornea, in addition to other characters which

are not discerned in fossils. They live in

deeper water, from 134 to 1269 m (Thle 1916)

and some are abyssal. It seems undesirable to

attach a varied and widely distributed group

of shallow-water crabs with a spatulate ros-

trum, large, apparently normal eyes and a

tymoline sternum to a minor group of small

deep-water crabs which, as we shall see, are

not their only descendants. I propose to

NEW CRETACEOUS AND TERTIARY CRABS 181

separate the Cretaceous genera Torynomma,

Divratiopus, Mithracites, Binkhorstia and pro-

visionally Eodorippe as a new family Tory-

nomidae which appears to be a more

“natural” taxon for them in the sense that its

recognition helps the discussion of tts rela-

tians, Those with Homoloidea and Prosopidae

remain to be clarified after farther studies of

their Jurassic representatives and, if possible,

af the Hauterivian “?Glaexsieria gteneuxi

(Van Straclen) mentioned by Wrght & Collins

(1972, p35). However, this single. frag-

mentury specimen, Of uncertayy provenance,

can no longer be found (R, Forster, pers,

comm. July 1980). Relations to Dramiidac

and Dynomenidac with which their living

descendants have been campared do not

appear to be close. The Torynammidae are

probably ancestral to Tymolidae (Cymono-

minae+Tymolinae) and possibly also Dorip-

pidae and Palicidae. similar to relations

depicted jn Bouvier's phylogenetic diagram

(Bouvier 1897, A. Milne Edwards 1902,

p,106) where their place is taken by unspeci-

fied “Dyhomeniens”.

Diagnosis of the family Torynommicdac:

Carapace square, rectangular or pentagonal in

outline, convex, front spatulale, projecting,

nal strongly deflexed; regions well marked by

grooves including the braachiocardiac; lateral

margins not sharp, side walls steep, eyes well

developed, retractable into shallow orbits.

Sternum triangular anteriorly, oval in outline

posteriorly, with the last sternites vertical and

chevron-shaped, It resembles the sternum of

the Tymolinac and Homolidae rather than the

configuration of the sternum in the Dromiaces.

Where known, the gonopares are coxal (pedi-

treme). Chelipeds subequal, secand and third

pereiopods long and strong, fourth and fifth

Cor the fifth only) in dorsal positioly and much

reduced, Abdomen with first somites exposed

dorsally. Cretaceous (Aptian to Maastrich-

rate).

Toryanmora Woods, 1953

Torynomma (Torynamma) flemingi nov. sp.

FIG. 9

Derivation of name: After Sir Charles

Fleming F.R.S,, Who has made outstanding

contributions to the palaeentological know-

ledge of New Zealand.

Holotype material:

Wellington, No. VA122.

Locality: Koutu Pojnt, Hokianga Harhour

(Loe. V2114). New Zealand.

Vietoria University,

Ave: Upper Senonran-Maastrichtian, Mata

Series.

Description: Carapace slightly convex,

approximately square in general outline, about

30 mm long and wide, Anterolateral margins

almost straight, posterolateral margins which

are damaged were slightly convex, width of

carapace across antero- and posterolateral

murgins was about equal but reduced about

middle of its length. Orbits large, very shallaw;

orbital margin struight, transverse, Extra-

arbital tooth coniesl, pointed, directed

diagonally forward, outward and upward.

Regions und lobes well marked, One small

tubercle on anterior mesogastric lobe, one

painted tubercle on its centre. Pasterior gastric

pits clearly marked. All other spinoge tubercles

arranged symmetrically: } on each side of the

hepatic, metagastri¢ and cardiac Johes, 2 on

cach protogastric and epibranchial lobe. Bran-

chial regions granulate. Carpus and merus of

the cheliped have sharp dorsal ridges. Cheli-

peds robust, subequal, Fourth and fifth pereio-

pads very weik.

Remarks; This species differs from T. quad-

rainm Woods (Fig. 8) in its size and the shape

ef the carapace which is flatter and has a

squarish outline. The spines on the surface

are more Hume;rous and much more prominent,

Paratoryuomima nov. subgen,

Type species. Torynamma (P.) denratum

nav, sp,

This subgenus differs from Terynomrna

Woods in its flatter and wider carapace with

a less deflexed rostrum and a strongly and

evenly granulaled surface, Its most obvious

difference i4 scen in the prominent antero-

lateral extraorbital teeth which are triangular,

directed forward and outward, and mark the

ercatest width of the carapace, The chelae

are more slender and elongate and the

chelipeds are longer, It differs trom Biora-

tiapuy by its almost straight fronto-orhital

margin and slightly converging posterolateral

margins hut resembles it in its granulate surface

sclupture und clongate chelae.

Torynomma (Paratoryuomma) dentatam nov,

FIGS 10-11, 20

Derivation of naine fram the conspicuously

dentate Fronte-orbital margin.

Marerial) Holotype P22930 and Paratypes

P2793) (tacality 1), P2293, P22941,

182

P22943 (Lue, 2); P22944 (Loe, 3), P22942

(Loc, 4), Collected by H, Daily 1954,

Localities: South coast of Bathurst Island,

vorth of Darwin, Northern Territery, Beach

cliffs and shore plattorm, Loc. I-3 are 16-25

km SW of Bathurst Island Mission. Loe, 1:

2.5 km E of Moonkinu Creek, Loe, 2:

Meadinga, E of Moonkinu Creek, Loc. 3:

Pouplimadurie Point, about 4 km E of Moon.

Kinu Creck; Loc. 4: Palliamundery Creek,

ceutral south coast, 35 km W of Bathurst

Island Mission,

Age: Upper Cenamanian, Bathurst Island

Formation, Moonkinu Member, from 3 tm

above to 5 fm below “Tapara Bed” with

Acanthoceray etc. (see Wright 1963, p,612)

at Loc. 1-3. Also From Lower Turonian, upper

part of Bathurst Island Formation with

Collignoniceray cf woolvari (Mantell); Lov.

4, All from glauconitle sands and elays.

Preservation. Most of the & specimens

examined are exceptionally well preserved aud

most were almost complete when embedded

in the sediment but the shell is in various stages

of decortication, The fragile shell and forma-

tion of incipient concretions uround Lhe bedies,

a common feature of the preservation of

decapod crustaceans in clays and sills, makes

complete preparation difficult There is little

distortion and most specimens show little

maverent between the carapace ai the rest

of the body, In several specimens a wap of

a few mm belween carapace and abdomen and

opening of the pleural suture tndivates that

they are probably moults, Seven specimens

are preserved In grey silly clay, one in glau-

conic sand, There is no doubt that they

lived where they were buried,

Deseriptions Carapace rectangular in outline,

wider than long, with a straight fronte-orbital

margin; gently convex longitudinally and

almost flat transversely, No disinct lateral

edge, side walls vertical; posterior maryin

sinuous. Front projecting only 4 short distiinee

forward but defected downward, with median

groove and pair of short basal spines, Pointed.

conical, supraorbital spine ahout eqnidistani

fron) front and conspicuous extraarbital~

anterolateral tooth. This is triangular im outline,

with flat surface, drawty out inte a long,

sharp, anterolaterally directed spine. Its

anterior margili bears 3-4 small lubereles ani

its tip is cranulated, Surface of carapace uni-

formly granulated. with only few more peo-

minent tubercles and few smoother arcas such

M. k GLATSSNER

os furcows and surfuce of anterolateral teeth-

Cervienl, hepatic and greater part of the

branchiocardiac lirrows about equally well

marked, Another posteriolaterally directed

groove vwonees ¢ervicd) and branchiocardiac

irrows and divides epibranchial lobes Meso-

ahd melabranchial lobes divided medially by

a longitudinal groove extending through the

faintly dclimited urogasirié lobe into the

cardiac region. Meso- and metrahranchial

tohes confluent. Orbits very larye and shallow,

vyestalks unusaully robust with smooth sur-

face. In one specimen a part of what appears

to be an antennal stalls projects forward from

helow the supraorbital tooth far about half the

distance separating front from anterolateral

tooth, Its proximal portion cannot be freed

withoul Gamage to the anterior pun of he

carapace.

The shape of the sternum (Fig. 11) 1s

distinelive. It is generally flat bur with sternite

7 (and consequently also 8 which js not pre-

served) turned upward, All sulures eacepl Ty 2

and 4/5 complete and crossing the midline

End of female abdomen extends lo a ridge on

sternite 4-5. Maly abdomen unknown, Gono

pores could jot be fecoenised with certainty

in this species. A third maxilliped preserved

in one specimen shows the ellipticul outline

of the merus, with subterminal articulation of

the carpus. Chelae of the P! subequal, with

clongate rectungulur propodus, covered wilh

spiny yerinylitions which tend to be aligned

in 2 rows Of ils Upper edge, Fingers as long

as the propodus and gently curved. Fixed finger

deflexed slightly dawnward, Merus and carpus

spinose, P2 and P3 about cqually strong and

long, With upper and lower rows of spmes on

the podomeres, Their length exceeds 20 mm,

with a diameter wf up te S mm, P4 and PS

thin, eylindcieal, with a diameter of ahour 1

in. smooth, articulated above the bases of

the Ps.

Divratiopus Waods, 1953

Type species PD salebrosay Woods

Dioratiopas Woods, 1953, p, $2) Wright & Collins

1972, p. 44. 34. 42

Yoritiopas Woods, Glacsener 1969, p. RAV? [erro-

Hioous spelling 1

Ghicawnerta Weight & Collins 1972 (non Takeda &

hiyake 1964), p. 34 17.

Glacswerellt Wright & Collins 1975, p, 441.

As noted hy Writht & Collins (1972, p, 33),

“the penera Glaessneria nov. and Dieratiopay

Woods are closely allied, The authors state

that the species of their new. genus ure dis-

NEW CRETACEOUS AND TRRTTARY CRABS tks

linguished from the Australian Dioratiopus

by being “much flatter in both transverse and

longitudinal section” They “lack the infer

oblique sulcus on the mesobranchial area

and have more strongly apinose frontal areas”.

The diagnostic validity of these characters must

be questioned, While some of the English

species are much flatter than the Australian

type species, this is not correct for the Euro-

pean type species “G.’ spinosa (Van Stfaelen

1936) which is more convex transversely and

unly insiynifizantly less so longitudinally,

except for the raised sides of its rastrum, The

oblique furrow on the branchial area is present

in Dioratiopuy, though possibly less pro-

noutived Jaterally where iL joins the branchto-

cardiac sulcus. ‘The generally weaker

development of carapace furrows in Diora-

tiopus cannot be considered as a reliable

generic character, and the same applics to the

less “spinose frontal areas” which are almost

without spines in several European species.

Small basal rostral, supraorbital and extra-

orbital/anterolateral spines are present in

Dioratiopus. The generic identity of Europea

und Australasian mid-Cretaceous decapod

crustaceans 1s not anomalous but is found in

Homolopsis, Notopocorystes and Hemioon

among the Brachyura and in Macrora. The

speeies. Homolopsis dawasonensis Bishop,

1973, which does not have a linea homolica

was considered by its authar to resemble

Homolopsix depressa Carter but to differ “by

being even less ornamented (haying no

ureoles), having a continuous sagittal ridge.

having more inflated branchial regions, and a

broader cardiac-intestinal region” (Bishop

1973, p, 20). These are specific differences

from “Glaexsnerina” depressa which is a

Dioratiopus, Bishop's species extends the range

of this genus to the Maastrichtian Pierre Shale

of Montana.

Diorariopus salelrasus Woods, 1953

FIG, 12, 12A

Diavationts salebrosus Woods, 1953, p. 53, nl 2.

fix, 4, 5, lext-fig 2.

Doratlapay salebroves Woods, Cilaessner 1969, p-

R492, fig, 704 12)

Materialy One specimen collected ancl

peesunted by H, Wopfner and DB. Scott on

hehall of Geosurveys of Australia No, (22953.

Leeallty: Wooldridge Creek ( =Fossil

Crevk), a tributary of the Alberga River, about

40 km NW of Oodnadatta, South Austraha.

Age: Upper Albian, Marree Formation (See

N. H, Ludbrook, Bull, 40, Geol. Survey 5,

Aust, 1966, ». 38, Map 4).

Remarks: The specimen is preserved ji part

ol # hard coneretian as an exlernal mont,

showing the almost complete carapace and

fragmentary pereiopods, lt agrees completely

with the holotype in type in size, shape aiid

ornamentation,

Dioranapus sp,

FIG. 21

Material; One specimen, P22928_ collected

by B. Daily 1954,

Locality: South coast of Bathurst Island N

of Darwin, Northern Territory, Poupanderi

Point, about 16 km SW of Bathurst Island

Missican

Age: Upper Cenomanian, Moonkinu Mem-

ber of Bathurst Island Formation, within

about | m below the base of the “‘Tapara Bed"-

Preservation, A poorly preserved carapace

in a fereuginised concretion containing alse

scattered remnants and external moulds of

perelopods,

Deseription: Carapace sibrectangular, sides

slightly converging toward the front. About 21

mm long, 16 mm wide and 7 mm high, Sur-

face gently rising, for about S mim from byse

of rostrum, generally fit longitudinally, gently

convex transversely. Greatest width appears to

be at level of posterior end of cardine revion.

Regions of carapace as in lype species; spines

apparently placed as in Mumnoalopsiy edwardsi

Bel] ‘but almost obliterated hy erusian and

probably originally less prominent, Surface

finely granulated. Orbital depressions below

the heputie lobe, stnailer than in the type

species. Chela with rows of granules on pro-

podius and carpus and with slender, curved

dactylus.

This species differs from AL ypinalese an

some details of outline and Jn its weaker

ornamentation, ‘The specimen is insufficiently

preserved for a specific diagnosis hut the

presence of an additional species in the

Bathurst Island Formaticn is of interest,

Eadorippe nov ger

Type species E. spedeni nov, sp,

Diagnosix: Characters as described for the

type species.

EFodorippe spedent noy. sp.

FIG, 14, 13A

Derivation ef tame After Dr [. Speden,

Geological Survey of New Zealand, whe sug-

12. Dioratiopus salebrosus Woods, Artificial cast of carapace of specimen P 22933. x2.

13. Eodorippe spedeni nov. sp. x2.

14. Rhachiosoma granuliferum (Glaessner). x1.

15, 15a. Pororaria eocenica nov. sp. Holotype, 15—dorsal view, 15a

16. Pororaria eocenica nov. sp. Paratype DC 361, x2.

frontal view. x2.

NEW CRETACEOUS AND TERTIARY CRABS 185

10 mm

{O mm

Fig. 14A. Rachiosoma granuliferum (Glaessner), Diagrammatic reconstruction of carapace.

Fig. 20, Torynomma (Paratorynomma) dentatum nov. sp, Paratype P 22936, sternum and appendages,

showing tip of mandible, basal parts of Mx3, P 1-3; right side reconstructed in outline.

Fig. 21, Dioratiopus sp. Carapace reconstructed.

gested the investigation of specimens from

New Zealand and assisted with information,

Material: One specimen, N.Z.G.S., AR 675.

Collected by Mrs J. Wiffen.

Locality: Stream boulders from bed of

Mangahouanga Stream, a tributary of the Te

Hoe River, from between bridge and waterfall.

Loc. No, N 104/f 909, Grid ref. N 104/

261088.

Age: Campanian-Maastrichtian (Pripauan-

Haumurian).

Preservation: Carapace showing dorsal

aspect and left flank almost completely pre-

served, with fragments of shell adhering to

surface of internal and partially preserved

external mould.

Description: Shell thin, carapace transversely

oval in outline, very moderately convex longi-

tudinally and transversely. Greatest width

across mesobranchial and cardiac lobes. Ros-

trum long and narrow, spatulate, pointing

forward; small granules on each side of its

18h

base, upper surlace with a longitudinal

Wepression, lower surface ridged, Fronto-

orbital aargin long, transverse. [ts mer

portion, occupying Jess thin half its wadth

ends laterally in a small, gutter-like depression;

Guler portion has i smeoth rounded,

prontinent ¢die. Infraorbital margin projects

hevond upper surface, orbital depressinns

large wnd shallow aud no suborbital tooth

was observed, Extraorbital-aiterolateral teeth

turn sharply forward, ending in short, pointed

spines, Rounded anterolateral margin bears x

small hepatic spine and leads to a pronounced

sinus mW) whith cervical and hranchiocurdiac

furrows ineet, continuing down the think 4s a

single straighe graave. Behind the incision there

is u shore, sharp ridge. It beoins with a shor

spine and is difected in an outwantly concave

curve backward and outward, slightly above

the rounded true later) carapace pefiphery

Carapace narrows Slightly behind end of ridge,

Posterolateral anil posterior margins sinuous

and toarked by a smuoth rilee Concave

median part of the posterior margin

short, Surface of catapace prominently marked

by transverse furrows aml few tubercles.

Cervical furraw sinuous and medially inter

rupted; hranchiocardiac firrows straight, con.

vergent bul become uaclesr neir the cardiac

region. Between ¢ervical and branchlocardine

furrows a pair of lnterimedlate oblique grooves

are the Most distinctive charaeter ol his cari-

pace pallern. They are literal extensions of a

groove heiween the meso ansl metagastrie

lobgs which are bisected by a weaker median

(lonwitudinaly furrow. Anterior and posterior

portions at the deesal surface are undivided by

gronves and are convex on éach side. Proto-

Bastfic lehes bear three tuhereles cach, spaced

whowl equally along an ure in front of the

cervical groove. leading to hepatic spine,

Mesogastrie Jobe, hounded by straight lines,

extends a long and very narrow tongue for-

ward, An elongate anterior and a shorter

posterior cpibronchial lebe on tach side, the

interior ending in a small marginal tubercle

iv the junetion of the main transverse grooves,

the posterior if shorter, obtiquely triangular in

outing, and sharply delimited from the meta-

gastric lobe, A faint, medially interrupted,

Transverse ridge and sume granulation on the

anterjor part af the i}l-defined cardiac regan

Surface minutely eranulated, with seme coarser

griinules on the Wesebranchial lobes.

Kemarkes There are some similarities in

stapes of the carapace anil the orbits between

M, F. GLAESSNER

(he New species and Milhracites vectensiy

Ciould from the Lower Aptian of England,

The differenees in the pattern of the transverse

furrows, the shape of the mesogastric lobe,

the hartow fostrum and the lack of the coarse

omamentation in Eodorippe justify a generic

istiniticon,

Svitemtatle position; Withers (1951) placed

Mithracites in the Prosopidac, a view rightly

criticised by Wright & Collins (1972, p, 40).

They point with some justification to certain

similarities With “Glaessneria”, here placed

in the synonymy of Dioratiapuy, and conse-

queauy include it in the family Cymonomidae,

The Late Cretaceous mew genus bas some

similarities with Cymonominae, The lack of

information on the morphology of the ventral

side of the cephalothorax of Eoderippe makes

its placing in a modern classification difficult.

In the «bsence of more complete specimens we

cannut decide whether this new genus ix pedi-

freme or sternitreme ancl whether it is oxysto-

matous, Despite the absence of such informa-

lion the striking resemblance between the cara-

pace of Eodorippe and the genus Dorippe

cannol he disregarded. ft is seen not only in

trivial generalities of shape and ornamentation

which can be due to common convergences

bul in details which are unique and cannot

he dismissed. The sinudsity of the wide

posterjor-posterolateral margin can be inter-

preted a8 indicating a position of the third and

fifth perciopods similar to that in Dorippe (the

hases uf the third pereiopods do not affect

the shape of the carapace margin), The lateral

convergence of the cervical and branchio-

cardiac grooves resembles closely the pattern

in several species of Dorippe (D. Jacchine

Herbst, 8. japonica von Siebald, OD. granulate

deo Hain) while the intermediate transverse

xroove appears to be present in D, dars/pes,

The position and shape of the shallow orbits,

the divided supraorhital margia and the extra-

orbital teeth ave also similar. If the classifi.

cation of Guinot (1978) is followed and the

Pulicidae are placed with the Dorippoidea,

some resemblances between Eodorippe and

Pulicus Philippi, 1838 become significant: the

great width across the (nesobranchial lobes,

the unusual multiplication of the transverse

froaves, afd the development of a sapittal

Incsogastnic and metagastrie furrow, Significant

differences ave the appurent absence of the

praminenc infraorbital teeth of Derippe and

the shape of the rostrum, ‘This shape ovakes it

Unlikely that Evderippe had resched the oxy-

NEW CRETACEOUS AND TERTIARY CRABS

stomatous condition of Dorippe with — its

dorsally visible exhalent opening. It agrees with

this structure in the Tymolidac and Torynom-

midae. The known characters of Eodorippe

suggest a derivation of the Dorippoidea from

Tymoloidea, This hypothesis remains ti be

tested by » study of the still unknown ventral

structures of the cephalothorax of Bodorippe.

It js tentatively attached to the Family Tory-

nommidae,

Family Portunidae

Rhachiovema eranuliferim (Glaessner, 1960)

FIG, 14, 14A

Portunites granulifer Glaessner 1960, p. 21,

pl. 3, fig, 7 text fig, 9,

New locality: Coustal cliff at Pororari, 2.4

km N of Punakaiki, Grid ref $37/723,

e85231 8.

Material and preservation: The incomplete

left half of a carapace, broken from the right

half of the front to the posterior margin above

the: fifth left pereiopod, The anterolateral teeth

2-5 are damaged, Mast of the shell surface is

preserved. Canterbury Museum, Christchurch,

New Zealand, Nozfe 9, coll, R, S. Allen,

Feb, 1935.

Age: Upper Focene, Kaidtan-Runangan.

The holotype was from the Middle Eocene,

Remarks; Purther studies of the type species

of Portunites (P. incertus Bell) suggest that

the Original generic assignment of the species

eranulifera was inuppropriate. Prominent

lateral spies are equal to almost half the

width of the carapace in Rhachiosoma bixpino-

yum Woodward, 1871 from the Lower Eocene

London Clay, but less than a quarter of

that width in R, granulifera. However, the

orbits and carapace sculpture are similar, The

new, fragmentary specimen has weaker and

probably fewer tubercles on the carapace

surface than the holotype bur until new and

more complete material is found, these

differenees are insufficient for the establish-

ment of a new taxon, The classification of these

fossils should be reviewed when the ventral

aspect and pereiopods are known,

Family uncertain

Pororaria nov. gen.

Type species P, cocenica nov, sp.

Diaenosis: Characters as described for the

Type species.

Pororaria cocenica sp. nov

FIGS 15, 15, 16

Marerlal; Two almest complete carapaces-

Holotype (including right chela). New Zealand

Geological Survey collecitan DC 360, paratype

NC 361, Also fragments of carapaces, chelne

aid walking legs and one carapace with both

chelwe: Canterbury Museurn, Christehurch,

New Zealand, Na_ 2fe 31-38, coll R. 8, Allen

Feb, 1935,

Locality: Cliffs al Porotari, 24 km Not

Perpendicular Point, Punakaiki (fe 71-38);

800 m S$ of Perpendicular Point, Map Sheet

S 37/735, NZ Geol. Survey locality

GS (0490 (DC 360-361)

Axe-> Upper Eocene. Kaittun-Runangan,

Description; Carapace as long as wide. tut

line oval ta hexagonal, very slightly convex

to flat surface smooth with localised concen-

trations of granules. Pront with a median

fgtch aid on cach side ) strong and 2 weak

teeth, Orbits as Wide as the front, with supra-

orbital yeauulations and 2 nolehes, with a gap

between the large antennal base and an tfra-

orbital tooth. Antennular bases folded back

obliquely, About 5 anterolateral teeth, obscured

by marginal granulaticns, Posterolateral

margin starts from a ridge behind last tnteral

loath hut not delineated on the inflated meso-

branchial lobes. Cervical groove well defined,

starting from posterogastric pils and

Uelimiting on cach side in three forwardly

eonvave arcs the mesogastric, protogastric and

heputic lobes, These are equally well defined

by hepatic grooves, There ure couieal tubercles

on hepatic lobes; groups of spinose granules

on meso-, proto- and metagastric. efi-, Meso-

and metabranchial, und eardiac lobes. Epi-

branchial ficld of granules has an unuswal

U-shape which resembles similarly placed

granulations in Dakelicaneer Rathbun, As

in this genus, a branchwcardiac groove

crosses rounded lateral margin behind

this granulated lobe. Urogastcie lobe finely

pitted and rectangular, cardiac region broadly

hexagonal. Posterior margin has a strong,

granulated ridge wilh » sieht median forward

bend, Chelipeds are sirong and heterochelous.

Carpus with spine near its inner distal angle.

Inflated propodus has smooth twner and

Pranulatcd outer and upper surfaces, Granules

tend to be arranged in longitudinul rows.

Fingers shorter than the upper length of the

propodus. strong minutely granulated, grooved

188 M. F. GLAESSNER

but otherwise smooth. Walking legs preserved

as scattered fragments which are thin and long.

Systematic position: In the absence of com-

plete pereiopods and of the sternum it is diffi-

cult to reach a definite conclusion about the

assignment of this new genus to an existing

higher taxon. It resembles the less advanced

Portunidae such as some Carcininae (Necto-

carcinus, Carcinus) in the general shape of

the carapace and in some characters of its

fronto-orbital region, Nectocarcinus shows a

similar transition from anterolateral teeth to

groups of spiny granules. The chelipeds are

also similar. Thin, long legs do not occur in

Carcininae and the lobes of the posterior half

of the carapace are different. There are also

resemblances with Atelecyclidae among the

Corystoidea but the relevant details of the

fronto-orbital region are not well enough pre-

served in the genus to allow a definite

conclusion about portunoid or corystoid

affinities; the configuration of the postero-

lateral portion of the carapace does not favour

the latter but the chelae are cancroid, A

similarity of the carapace with that of Avitel-

messus Rathbun does not apply to its median

portion which shows a corystoid pattern.

Avitelmessus is very close to Dakoticancer.

As Guinot (1978) remarked, these genera

should not be assigned to the Dromiacea.

Whether Pororaria is related to Corystoidea

or Portunoidea remains to be elucidated. Until

further evidence is found, the new genus is

tentatively placed in the superfamily Por-

tunoidea.

Family Panopeidae

Panopeus H. Milne Edwards, 1843

Type species P. herbsti H. Milne Edwards

Panopeus whittenensis nov, sp.

FIGS 17-19

Material: More or less complete carapaces,

chelae, fingers, and fragments of legs, Holo-

type P22935, paratypes P22938, 22939,

22946-22950.

Localities: Whitten Bluff, S of. Christies

Beach, 28 km SSW of Adelaide (type locality

and most common occurrence). Also from

Fig. 17. Panopeus whittenensis nov. sp. Holotype,

x3. Posterolateral margins restored.

Fig. 18. Panopeus whittenensis nov. sp. Paratype

P 22938, x2.

Fig. 19. Panopeus whittenensis nov. sp. Right

chela, specimen P 22939, x2.

NEW CRETACEOUS AND TRRTIARY CRABS

Maslin Bay. about I5 km turther south,

Coastal cliffs on the E shore of Gulf St

Vincent (P22438, coll, Dr M, Buonajuia)

Age: Upper Eocene, upper Tortachilla

Limestone 4nd hase of Blanche Point Porma-

tion (= “Transitional Marl"). Planktanic

foraminiferal zone 15.

Preservation; Some complete and same

broken carapaces without branchiostegates,

sternum, abdomen, or ativehed appendages,

The propodus of the cheliped may have the

dactylus and parts of the carpus attached but

more offen it is disjointed, Small fragments

of perciopods apparently belong to this species,

The only other decapods found with Panopets,

in a rich shallow-water fauna of cirripeds,

bryozoans, brachiopods, echinoderms, serpulid

worm lubes (some attached to carapaces and

chiws of Periopeds) and numerous mollusca

are one incomplete dromiid carapace (Drurni-

fires? sp.J, a few claws of an oxyrhynchous

erab, and chelae of a callianassid.

Description: Carapace slightly wider than

long, convex. Frontal margin straight, with

median indentation and transversely grooved

and finely granulated edge. Orbits well

developed, with inner supra- and infraorbital

teeth, evenly granulated edges and 2 supra-

orbital fissures. Anterolateral margins with 5

conical teeth of which the fourth is the

strongest and mast prominent and the fifth the

weakest, Posterolateral margins converging

hackward. Posterior margin wide, with raised,

faintly granulated rim, Main regions of the

carapace surface well marked by shallow

grooves, Posterior gastric pits clearly visible,

Surface appears to be smooth when well pre-

served, becoming granolated with decortication

by weathering, Some mdividual variability: in

omamentation. No remarkable features in the

pattern of regions except perhaps strong

development of the epigastric and metagastric

lobes, Right chela strong, propodus smooth,

with a very faint depression below the upper

edye and two rows of pits above and along

lower cdge of fixed finger. A tow of irregu-

larly sized and blunt teeth on its upper edge,

Lower edge of the propodus and finger strongly

curved to fit snugly along fhe anterior margin

cephalothorax. The carpus fs square.

Measurements (in mm): Lengths and widths

17.8 and 22.5, 22 and 26, 20.5 and 23, 22,5

and 28. In the carapace which is 20,5 mm tong,

the frontal margin has a half-width of 4 mm

and the orbit was 4.5 mm wide In a cara-

isy

pace which wis about 20 mm long and 24 mn

Wide. the orbit was about 5 mm wide A

large propodus wilh fixed finger is about 35

mm long and 18 mm high.

Remarks: In the absence of any parts of

the ventral surface of the cephalathorax or

appendages other than the large claw, the

precise systematic position of this ctab remains

in some doubl, The absence of transverse

raised lines ou the carapace would distinguish

it from the living species of Panepeus for

which their presence ts a Convenient diagnastic

character. tt would not necessarily exclude it

from the evolubonary lineage of this genus

which has been reported from the Paleocene

and Eocene. The new spocies as far as known,

16 morphologically closest ta Parnapeus and

therefore assigned to it, pending diseovery of

other still missing parts.

Phylogenetic conclusions

The phylogenetic significance of several of

the new Cretaccous and Tertiary crabs here

described has been briefly mentraned, It can

now be considered in the framework of the

adaptive radiation of the Brachyura (Fig. 22,

see also Glaessner 1980). This updated version

of a phylogenetic diagram which & first puh-

lished 50 yeurs ago (Uilaessner 1930; L960,

Fig, 22) incorporates some of the results of

the monogeaphic work of Wright & Collins

(1972) on British Lower Cretaceous crabs

and reflects the new classification of ihe Brach-

yura by Guinot (1977, 1978) and other

important studics which are considered jn it,

Certain modifications and ce-acrangements of

this classification are suggested ss a result of

the present investigation.

The new family Torynommidac may have

evalved ultimately from the family Peosepidae

of the Homolodromividea, as implied by

Wright & Collins (1972) and probably from

archacobrachyuran descendants, the Homo-

loidea, iv Late Jurassic-Eacly Cretaceous or in

Mid-Cretaceous time, Their living descendants

are related fo them in a manner depicted with

remarkable foresight by Bouvier as early as

1897. They also may have given rise to the

Late Cretaceous Carcineretidae which acquired

an early adaptanon ta swimming. From similar

origins in the podotrematous Homoloidea the

well docurnented Necrocarcininac-Calappinae

lineage (Férster 1968) and possibly Orith-

yidae (sce Guinot 1978, p.255) evolved and

and eventually attained the fieterotrematous

trade. Their Mid-Cretacemus descendants, the

190 M. F. GLAESSNER

HETEROTREMATA. ssi THORACOTR.

PODOTREMATA |

ARCHAEO | BRACH. DROMIACEA

\ Cc

er rerogoRO*_co®

a 2

4X nh abgey, p>

100

F HABITS &

c HABITATS s] m2

B: BURROWING at Sr csk

150-7 C: CONCEALMENT Fram cape ot re

L:LAND

z S: SWIMMING

200

Fig. 22. Adaptive radiation of the Brachyura.

Superfamilies (and lower taxa marked with *): LEU Leucosioidea, MAJ Majoidea, PAR Partheno-

poidea, COR Corystoidea, POR Portunoidea, DOR Dorippoidea, CARC* Carcineretidae, TYM

Tymoloidea, RAN Raninoidea, ORI* Orithyidae, CAL* Calappidae, NEC* Necrocarcininae, HOM

Homoloidea, H/DR Homolodromioidea, DROM* Dromiidae, DYN* Dynomenidae, XAN Xanthoi-

dea, GEC Gecarcinoidea, GRAP Grapsoidea, PIN Pinnotheroidea, HEX Hexapodoidea, OC Ocypo-

doidea. Geochronometric (in million years, my) and stratigraphic scales at left. N Neogene,

P Palaeogene, UC Upper Cretaceous, LC Lower Cretaceous, UJ Upper Jurassic, MJ Middle Jurassic,

LJ Lower Jurassic, Note that top of Paleocene is shown within Palaeogene, and Albian and Ceno-

manian are marked below and above line dividing Cretaceous. Dotted lines mark the three periods

of major diversification of the Brachyura.

Raninidae, adapted to burrowing and remained

at the podotrematous grade, The discovery of

Eodorippe strongly suggests a Late Cretaceous

origination of the heterotrematous Dorippidae

from Tymoloidea, as foreseen by Bouvier. This

is still subject to confirmation by more com-

plete material.

The origins of the remaining Heterotremata

are still unknown, probably diverse, and dated

mostly Late Cretaceous to Early Tertiary.

Wright & Collins (1972) conclude that the

Xanthidae were derived from Dynomenidae

in Late Jurasic-Early Cretaceous time, This

derivation cannot apply to other Heterotre-

mata which show no signs of origination from

Dromiacea or indeed of pre-Tertiary existence.

It is possible that further studies of Pororaria

may clarify relations with or between Por-

tunoidea and/or Corystoidea (a prior synonym

of Cancriformia). Some members of these

two superfamilies show a dichotomy between

habits and adaptations for swimming (as in

Portunus) as opposed to burrowing (as in

Corystes). The portunoid adaptations for

swimming do not seem to be derived from but

rather heterochronously convergent to those of

the Carcineretidae. The burrowing habit of the

Corystidae is generally considered as a con-

vergent or possibly parallel adaptation com-

pared with that of the Raninidae. The origins

of the Leucosiidea and Majidea remain

obscure; their adaptations diverge distinctively

from those of any other group of crabs.

The Thoracotremata, at the highest grade,

include the land crabs and various successful

strand dwellers with a variety of habits, They

resemble the Xanthoidea more than other

Heterotremata but their origin, in the Late

Cretaceous or Early Tertiary, is cryptic.

As in all phylogenies, many questions

remain, but new material, particularly of

Mesozoic and Early Tertiary age, can now be

NEW CRETACEOUS AND TERTIARY CRABS ina

fitted more easily and rationally into the

framework of existing knowledge and classifi-

cation, Most importantly, the replacement of

the traditional but mostly ill-conceived “Scec-

tions” with a horizontal classification at the

highest level by grades, has improved our

understanding of the history of the Brachyura.

Acknowledgments

My thasks are duc fo Dr B. Daily, Depart-

ment of Geology and Mineralogy, University

af Adelaide, who collected the fossil ¢rabs

{rom outcrops on Melville and Bathurst Island,

Northern Territory, and established their

stratigraphic position; to Dr 1. Speden, Geo-

logical Survey of New Zealand; to the

authorities of the Victoria Museum, Welling-

ton and the Canterbury Museum. Christchureh,

New Zealand, and to Dr Mary Wade, Queens-

land Museum, Brisbane. for the loan of speci-

mens from collections in their institutions, to

Dr N. H. Ludbrook for ihe loan of a

specimet from South Australia and for infor-

discussions on British Cretaceous crabs, Dr

Daniéle Guinot, Muséum noational dHistaire

naturelle, Paris, discussed relevant aspeets of

her work with me and provided essential

literature.

All specimens with numbers prefixed P have

been deposited in the Sovth Australian

Museum, Adelaide, The photographs were

prepared by Mr R. Barrett, The skilful

drafting of Fig, 22 is the work of Misy A.M,

C. Swan. Geology Department, University of

Adelaide.

References

Ratss, H. (1957) Decapoda. /a: Dr H. G, Bronn's

Klassen und Ordnungen des ‘Tierreichs, 5, LAbt..

7.Buch, 12.Lief., 1505-1472.

Histor, G. A. (1973) Homolopsis dawisenensise

A new crab (Crustacea Decapoda) from the

Pierre Shale (Upper Cretaceous, Maastrichtian)

of Cedar Creek Anticline, Eastern Montana. J.

Paleont,, 47, 19-20, pi. J.

Bouvien, E. L. (1897) Sur ta classificutian. Jes

Orivines ct la distribution des crabes de la famille

des Dorippidés, Bull. Sac. philemath, Paris, ser,

8.9, p, 54-70,

Frupringe. R. sun. (1917) Desenptions of some

Oucensland Palavozoie and. Mesozoic fossils, 1

Queensland Lower Cretaceous Crustacea, Geol,

Survey Old. Publ, 260, 5-10, ;

PorsteR. R. (1968) Paruiecrecarcinus lbanotcus

n. sp. (Decapoda) und die Rotwicklung der

Caluppidae in der Krelde. Mint. hayer. Staais-

saniml. Pal. hist. Geol. 8, 167-195, pl. 13.

GiagssNur, Mo F. (1930) Beilrfage zur Stammes-

peschichle der Dekspoden. Paldons. 2. 12. 25-

42.

—~.— (1960) The fossil degupod Crustacea of New

Zealand and the evolution of the order Decu-

poda, N.Z Geol, Survey Paleant. Bull, 31, 63 p.,

Jol.

als (1969) Decupods in; Moore, R. C. feds

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(980) The adaptive radiation of the Brachy-

ura (Crastaces Decapoda). Absirjcts, Sect. 3,

26th Int. Geol. Congress (in press) -

Gornon. J. (1963) On the relationship of Dro-

miacea, Tymolinuc and Raninidae to the Bru-

chvura. @i: Whittington, H, B. & Rolfe, W. D, I.

ieds.) Phylogeny and evolution of the Crusta-

cea. Harvard Univ Muy. Camp. Zool. Spec.

Publ, 31-57.

Guteor. D, (1977) Propositions pour une nouvelle

classification ues crustacés décapades brachyures.

CR, Acad, Sei, Paris (D) 285. 1049-1052.

(1078) Principe d'une classification evolutive

des crustacés hrachvoures. Aull, biol, Prance

Belviqne, 142, 211-292.

(1979) Morphologie et phylogenése des hra-

chyoures, Aden. Afuy. Nat. Ais Neti, ma

112, 354 pp. [Received after completion of this

pupery.|

Henveasom, RB, A. (1973) Clarence and Rauku-

taara Series | Albian—7Santonian) Amimonodes

from New Zealand, 1 R- Sor, NZ, afl), 71-

123,

THie. J. EB. W. (1916) Die Decupoda Brachyuru

der Siboza Expedition. fl. Oxystomata, Dorip-

pidac, Sihows Expeditic, Uitkamsten 39h, tive

78, 97-158

MiLNeE Enpwarps A & Bouya, B. L. (1902)

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supervision of Alexander Agassia . . . by the

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Sumveid, Z. (1973) The systematic position of the

family Raninidae, Sysi, Zvi, 22, 625-32.

Vit Boapa. L. (1980) Deyppdodea (Crustices

Décapodes) diy Cénozoique méditerruneen, Ori-

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Paléont, (nvert,) 66(7), 51-66.

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Wooow are, H. 01892) Note on a new decupodaus

cruslaceun. Proopon ethernidges H. Woodw.

from the Cretaceous of Queensland. Proc, Lin

Soe. N.S.W. 7(2i- pt. 1, 301-304, p, 4,

Woovs. J, T. (1953) Brachyura [rom the Creta-

ceous of Queensland. Meni, Qld ATus. 13. 50-57.

Wricut, C. W. (1963) Cretaceous ammonites

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pp. 22 pl.

—— (1975) Glaessnerella (Crustacey Decapoda,

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192 M. F. GLAESSNER

Postscript

Via Boada (1980) reviewed the evolution of the

Ocypodoidea, tracing their origin to the Creta-

ceous genera Ophthalmoplax and Archaeopus. I

had previously (Glaessner 1969) referred the first

to the Carcineretidae and the second, doubtfully,

to the Palicidae. Subject to further studies, Via’s

views suggest interesting possibilities of exploring

evolutionary links between Ocypodoidea, certain

Dorippoidea, and Carcineretidae. When I received

his new data it became possible to identify a

Middle to Late Eocene crab from a limestone core

from the Ashmore Reef No. 1 Bore off the NW

coast of Australia (sent to me in 1968 by Dr P. J.

Coleman and the Burmah Oil Company) as at

least very close to Retropluma as described from

rocks of similar age in Spain, It lives now in deep

water in the Indian Ocean.

A NEW SPECIES OF CYCLORANA (ANURA: HYLIDAE) FROM

NORTHERN QUEENSLAND

BY ERIC VAN BEURDEN & K. R. MCDONALD

Summary

Cyclorana manya sp. nov. from Cape York Peninsula, northern Queensland, is described. It is small

compared with known congeners and has close affinities with C. brevipes and C. longipes.

A NEW SPECIES OF CYCLORANA (ANURA: HYLIDAE) FROM

NORTHERN QUEENSLAND

by ERIC VAN BEURDEN* & K. R. MCDONALD?

Summary

VAN BEURDEN, E. & MCDONALD, K. R. (1980) A new species of Cyclorana (Anura: Hylidae)

from northern Queensland. Trans. R. Soc. S. Aust. 104(6), 193-195, 28 November, 1980.

Cyclorana manya sp. nov. from Cape York Peninsula, northern Queensland, is described.

Tt is small compared with known congeners and has close affinities with C. brevipes and C.

longipes.

Introduction

In a partial revision of frogs of the genus

Cyclorana Steindachner, Tyler & Martin

(1977) described five new species and raised

the total to 10, highlighting the diversity

within the genus. We describe a further species

from northern Queensland. It resembles C.

longipes Tyler & Martin but is considerably

smaller than this or any other congener.

Methods

The type specimens are lodged in the

Queensland Museum (QM), and South

Australian Museum (SAM). Measurements

were obtained using a pair of Helios dial

calipers (to nearest 0.1 mm). Eye to naris dis-

tance (E-N) is the distance from the posterior

margin of the external naris to the anterior

margin of the eye. Internarial span (IN) is the

distance between the medial margins of the

external nares. Other measurements are as

defined and abbreviated by Tyler and Martin

(1975): HL = head length, HW = head

width, S-V = snout-vent length, TL = tibia

length.

Mating calls of two individuals were

recorded on a Uher 4000 report tape recorder

at a tape speed of 19 cm/sec using a Grampian

DP4 microphone. Air temperature was

recorded within 3 cm of the frog using a

Schultheis mercury thermometer. One call of

each individual was analysed using a Kay

Model 6061—A Sono—Graph audiospectrograph

set on a narrow-band (45 Hz band-pass), and

a response curve setting of FL—-1. This pro-

vided measures of call duration, band spacing,

lowest and highest frequency. Pulse repetition

rate and fundamental frequency were taken

* Department of Zoology, University of New Eng-

land, Armidale, N.S.W. 2351.

* Queensland National Parks & Wildlife Service,

Pallarenda,

from photographs (Polaroid B & W type 107)

of oscilloscope traces using a time scale of 2

msec/cm,

Cyclorana manya sp. nov.

FIGS J-2

Definition: A small species (male adults 27.2—

29.9 mm; female 27.5 mm) with short hind

limbs (TL/S-V_ 0.32-0.38). The head is

bluntly rounded and the eyes are large (E/ E-N

= 1.71). There is no dark head stripe from

the tip of the snout to the eye or from the eye

to the axilla.

Description: Holotype (QM J34886), an adult

male collected between Coen airport and Deep

Creek crossing 25 km N. of Coen township

(13°52’S, 143°12’E), Cape York Peninsula,

Queensland, by E. van Beurden, M. Sabath,

B. Easteal, M, Robinson and J, Sparkes on

17.1.1979.

Habitus stout, body globose (Fig. 1). Size

small. Head broadly triangular when viewed

from above, flattened and broader than long.

Fig. 1, Paratype of Cyclorana manya shortly after

capture near Coen.

194 ERIC VAN BEURDEN & K. R. McDONALD

Fig. 2. Palmar and plantar aspects of hand and

foot of holotype of Cyclorana manya (QM

J34886).

Snout rounded when viewed from above and

bluntly rounded in profile (HL/HW 0.89).

Nostrils inconspicuous and dorsally inclined.

Canthus rostralis slightly curved but not

prominent. Eye prominent, its width more than

3 times eye to naris distance. Upper part of

iris golden, lower part, silver/grey and an-

terior and posterior portions black.

Tympanum distinct except for upper and

posterior margins which are obscured by

supra-tympanic fold.

Tongue ovate, about 4+ free behind and just

over 4 as wide as gape, Choanae large and

widely spaced. Vomerine teeth present on

obliquely converging elevations, between pos-

terior margins of choanae.

Fingers short and unwebbed (Fig. 2) with-

out lateral fringes. Subarticular tubercles

prominent; paired nuptial pads on each thumb.

Toes slightly webbed. Webbing on medial

side of 5th toe does not reach subarticular

tubercle at base of penultimate phalanx.

Relative toe lengths 4>3>5>2>1. Prominent

inner metatarsal tubercles, twice length of first

toe (Fig. 2). Hind limbs short (TL/S-V 0,34).

Skin of anterior portion of thigh smooth;

that on posterior pitted.

Dorsal body markings of preserved specimen

consist of dark grey-brown irregular blotches

on lighter brown background. These blotches

diminish in size and intensity on flanks and

posterior parts of dorsum. A pale, unbroken

vertebral stripe runs from tip of snout to tip of

urostyle. A broad, light-coloured post-orbital

bar crosses head posteriorly at level of tym-

pana. Top of head dark grey-brown while

sides, extending down to upper lip, are pale

brown.

Ventral surfaces of body and limbs pale

cream, as is lower lip. Skin beneath vocal sac

darkly pigmented, and skin of abdomen trans-

lucent. Posterior region of thigh and flanks

pale brown with darker brown blotches.

Dimensions: S-V 29.9 mm; TL 9.5 mm; HL

9.2 mm; HW 11.2 mm; E-N 2.1 mm; IN 1.5

mm; E 3.8 mm; T 1.2 mm.

Variation; Two paratypes: a mature female,

QM J34888, and a mature male QM J34889,

were collected with the holotype. Twelve fur-

ther paratypes SAM R17420-R17424; QM

J36894—900) including nine mature males, and

three immature individuals were collected by

R. G. Atherton and K. R. McDonald at the

southern end of Coen air strip (13°46'S,

143°07’E) on 6-8.iii, 1979.

The S-V range is 27.2—29.9; the largest

specimen being the male holotype. The head

is consistently broader than long (HL/HW

0.82-0.96) whilst the nostrils are narrowly

spaced (E-N/IN 1.25-1.69), The hind limbs

are consistently short (TL/S—V 0.32-0.38).

Colour and pattern are variable. The colour

of the dark blotches on the dorsum varies from

light grey to a rich, dark brown-grey, The pro-

portion of the dorsum covered by these

blotches varies from about 55-85%. The

vertebral stripe varies in its conspicuousness

and the variation is not consistent with the

intensity of blotches.

All specimens larger than 25 mm S—V,

except the female, were males with pigmented

vocal sacs and nuptial pads. The single female

was gravid and contained about 100 eggs, each

about 1 mm diameter. Specimens less than

25 mm lacked eggs or male secondary sex

characteristics.

Mating Call: The call is a short plaintive bleat

of 1.1-1.3 sec. duration (Fig. 3). The domi-

nant frequency is about 2500 Hz and the call

consists of S—8 distinct bands separated by 328

Hz, and ranging 400-3000 Hz. Pulse repetition

rate is 294 pulses/sec., and the call is

repeated 10-16 times per minute. Calling males

were recorded and collected while floating,

legs extended, at the surface of shallow

A NEW SPECIES OF CYCLORANA 195

ENCY (kL!

FREOU

TIME anc}

Fig. 3. Audiospectrogram of mating call of Cyclo-

rana manya vecorded during rain at Coen Air-

port. (Air temp. 24.8°C, band pass = 45 Hz.)

temporary puddles,

during heavy rains.

24.8°C.

Breeding: The presence of juveniles in March

and the calling activity in heavy rainfall sug-

gests that this species is an opportunistic,

summer breeder, Little calling was heard on

nights when rain was light, and there was none

on the dry nights following that on which

recordings Were made.

Comparison with other species; Comparisons

are based on descriptions provided by Tyler &

Martin (1977), The most obvious difference

between C, maya and congeners is the S=V of

adult males which is 4.8 mm shorter than the

smallest adult previously reported, It also lacks

a head stripe from the snout to the eye and eye

to axilla, The range of B-N/1N overlaps only

C. longipes. Call characteristics are most

similar to those of C, brevipes Gunther, The

call duration of the tWo species is about 1 sec.,

und the dominant frequency has 3-4 side

in grassy depressions

Air temperature was

bands above and below it. The call of C,

manya differs from that of C. brevipes in

that the dominant frequency i higher and

band spacing is wider. Coloration most closely

resembles that of C. longipes except that dark

head pigmentation terminates at a broad, pale

transverse bar extending around the tympanum

and down to the axilla.

Four frogs (DT-D 0737-40) taken at

Lower Archer River on Cape York Peninsula

by J. Thompson in 1933 may represent a (orm

intermediate between C. Jongipes and C.

manya. Their E-N/IN ratios (1.22-1.25) and

bold head coloration are similar to C, lon-

gipes, S-V (32,2 and 40.7 for the two adults)

is intermediate between C. manya and the

larger C. longipes.

Etymology: ‘Manya’ is the Aboriginal word for

‘small in the local dialect (Wik-munken) at

Coen. This is appropriate for ihe smallest

‘water-holding frog’ described.

Acknowledgments

We thank J. D. Miller and Michael J. Tyler

for reviewing the manuscript. Drs Michael

Sabath, J. W. Winter and Janet A. Taylor also

provided valuable comments. E.V.B. was funded

by the Australian National Parks Wildlife

Service (grant for the study of Bufo marinus)

and COMALCO, and Ian Potter Foundation

trants to M. Sabath and S. Basteal. K.R.M.'s

work was carried out in the course of a

Melllwraith Range fauna survey (Dr J. W.

Winter and R, G. Atherton co-ordinators)

partly funded by the Australian National Parks

and Wildlife Service. We are also grateful to

the Donald Thompson Collection Administra-

tion Committee, and the National Museum of

Victoria for allowing us to examine the speci-

mens from Lower Archer Raver.

References

Tyrer, M. J. & Martin, A. A. (1975) Australian

leptodactylid frogs of the Cyclorana australis

complex. Trans, R. Soc. S. Aust. 99, 93-99,

(1977) Taxonomic studies of some Austra-

lian leptodactylid frogs of the genus Cycloraru

Steindachner. Rec. 8. Aust. Mus., 17, 261-276.

EARLY CAMBRIAN TRILOBITES FROM THE OFFICER BASIN, SOUTH

AUSTRALIA

BY J. B. JAGO & B. C. YOUNGS

Summary

Fragmentary trilobites, probably of early Early Cambrian age, occur in the Observatory Hill Beds

from the eastern part of the Officer Basin. The trilobites were recovered from limestone core at a

depth of 87.85 m in Marla-1, a stratigraphic hole drilled by the South Australian Department of

Mines and Energy. Their discovery allows the first reliable macrofossil dating of the Officer Basin

sediments in South Australia.

EARLY CAMBRIAN TRILOBITES FROM THE OFFICER BASIN,

SOUTH AUSTRALIA

by J. B. JAGo* & B. C. YOUNGs*

Summary

Jaco, J. B. & Younes, B. C. (1980) Early Cambrian trilobites from the Officer Basin, South

Australia. Trans. R. Soc. S. Aust. 104 (6),

197-199, 28 November, 1980.

Fragmentary trilobites, probably of early Early Cambrian age, occur in the Observatory

Hill Beds from the eastern part of the Officer Basin, The trilobites were recovered from lime-

stone core at a depth of 87.85 m in Marla-l, a stratigraphic hole drilled by the South Austra-

lian Department of Mines and Energy. Their discovery allows the first reliable macrofossil

dating of the Officer Basin sediments in South Australia.

Introduction

The Officer Basin is a large intracratonic

depression in western South Australia and

southeastern Western Australia (Fig. 1). The

main part of the S.A. portion covers an area

of approximately 100 000 sq. km. and contains

sediments ranging in age from Late Proterozoic

to Devonian in surface and near-surface out-

crops (Fig. 1). Subsurface outliers exist to the

east and south of the main basin (Pitt et al.

1980). The deep northern parts of the Officer

Basin may contain at least 6000 m of

sediments.

This paper reports the first trilobites recorded

from sediments in the S.A. portion of the

Officer Basin. The only previously recorded

macrofossil from this part of the Basin is a

single specimen possibly representing Biconu-

lites (Gatehouse 1976). Prior to the present

report, the only palacontological evidence for

ee ——

* School of Applied Geology, South Australian

Institute of Technology, P.O. Box 1, Ingle Farm,

S. Aust. 5098.

+ Geological Survey of South Australia. Present

address: South Australian Oil and Gas Corpora-

tion.

1 Harris, W. K. (1968). Continental-Sun-Exoil-

Transoil Munyarai No. 1 well palynological exa-

mination of cores. S.A. Dept Mines & Energy Rept

Book 754, Appendix 4 in envelope 979 (Cunpub-

lished).

2 Gilbert-Tomlinson, J. (1968). Fossils from Mun-

yarai No. | Well, Officer Basin, South Australia.

Appendix 7 in S.A. Dept Mines & Energy Rept

Book 979 (unpublished).

3 Vlierboom, F. W. (1973). Palynology and source

rock potential of core samples from the Conoco

exploration well Munyarai-1, Officer Basin, South

Australia. In S.A. Dept Mines & Energy Rept

Book 979 (unpublished),

4+Muir, M. D. (1979). Palynological examination

of microfossils from the Observatory Hill Beds,

Wilkinson No. 1 DDH, Officer Basin, South Aus-

tralia. Appendix 2b in S.A, Dept Mines & Energy

Rept Book 78/88 (unpublished ).

the age of any of the basin’s sediments came

from Devonian microfossils recovered from

cores in Munyarai-1!* and Early Cambrian

microfossils from the Observatory Hill Beds in

Wilkinson—I+, The specimens figured herein

are housed in the palaeontology collection of

the S.A. Museum; the catalogue numbers refer

to this collection.

Stratigraphy

The stratigraphy of the eastern Officer Basin

is summarized in Figure 2. The fauna discussed

in this paper was recovered from cores in

Marla—I (lat. 27°28.1'S, long. 133° 44.8’E), a

stratigraphic well drilled by the S.A, Depart-

ment of Mines and Energy in 1974 (Thornton

1978). A more complete section through these

beds was drilled during 1979 in Marla—1B

(Fig. 3): this well, located near the site of

+, +

OFFICER BASIN

(Area of outcrop and

shallow suberop} OBSERVATORY HILL A

(iyps, soeuson)

Wilkinson—1¥y

OFFICERY DI

BASIN SA jm~ienoms)

peat

KILOMETRES

o 100

0 yono

Lt MELBOUIINE

YILOMETRES:

Was cADME

Fig. 1. Locality map, Officer Basin.

198 !,

Boorthanna Formation

Isufsurtace Arckarnngs

Basin only)

Minsabie and Wartaona Beds

‘Munyarat Sequence’

(Subsurface only)

Carn Beds

Blue Hills Sandstone

Indulkana Shale

Mount Chander Sancstane

Sequence

Munda

PALAEOZOIC

Traior Hill

Sandstone

Mi Johns

Dongomerate

Cambrian

OBSERVATORY ‘Doves Anre

HILL. BEDS

Conglomerate

Gan)

3 Marit Sequefice

Marinoan

LATE <=

PROTEROZOIC

Fig. 2. Simplified stratigraphy, Officer Basin, S.

(modified after Pitt ef al, 1980),

Marla—1, intersected nearly 300. m and was

still in che Observatory Hill Beds when drilling

was stopped.®> Marla-1 well intersected

22,58 m of Observatory Hill Beds unconform-

ably beneath the "Early Permian Boorthanna

Formation, The specimens desoribed herein

are trom 87.85 m depth, Other, at present

indeterminate, tnlobite fragments have been

found at a depth of 333 m in Marla—-1B.

The Observatory Hill Beds in Marla-IB are

a flat lying sequence of predominantly fine-

grained, buff to grey, silty carbonates with

minor thinly interbedded calcareous siltstones

and sandstones, Above 176 m, caleite und

dolomite mudstones and boundstones are coni-

mon. with chert and fluorite occurring

throughout. Below 176 m to the total depth of

379 m, the section is predominantly dolomitic

and evaporitic mudstones with some bound-

stones, wackestones and packstones, Fine- to

medium-grained calcareous «and dolomitic

siltstones aod sandstones are interbedded

throughour, Fluorite is rare, bul secondary

chert and sulphides are common

" Benbow, M. C. (1980). Marla-1A, 1B well com-

pletion report. S.A, Dept Mines & Energy Rept

Book 80/22 (unpublished )_

"Lydyard, A. J, (1979). A petrographic study of

the sediments in seven Officer Basin stratigraphic

wells. S.A. Dept Mines & Energy Rept Book 79/55

(unpublished ).

B, JAGO & B,C. YOUNGS

Apart from algal mats and stromatolites

throughoul the sequence, the only fossils are

trilobite fragments. These are found oily at the

top of the drilled section and were recorded at

levels similar to those in Marla—l-

Unbke the Observatory Hill Beds in Byil:

Kagoora-l (Fig. |) which are considered non-

Marine (White & Youngs 1980), those in

Marla-!, —1B are interpreted as marginal

marine, The basal 200 m were deposited on

mudflats and in tidal channels which may have

been subjected to periodic exposure. The beds

above 176 m show an increase in marine

influence and were probably deposited in the

shallow, quiet waters of a lavoon on a broad,

shallow platform,

Valaeontology

Several trilobite fragments were recovered

from limestone core at a depth of 87.85 ni in

Marla—|, after having been discovered during

pelrographic work,” However, there are only

three small, fragmentary specimens on which

reasonable comment can be made. The small-

ext available specimen, P22981, is very small

(Fig. 4a) and may be wn immature form of the

speeies described below. However, the glabellar

furrows of P22981 seem to be shorter and less

distinct aud the anterior border is narrower

than in that species, Until more and better

material is available, it will not he possible to

identify this specimen.

QUATERNARY AND EARLY CRETACEOUS AND

2 EARLY PERMIAN |BOORTHANNA FORMATION)

(See Bantow, 1980)

EARLY CAMARIAN—OBSERVATORY HILL BEDS

f Carpandtis (predaminaniy miudstonesy with

f imerbedderl silty camanaias, salearcnus

seirstunes and sandstones

Algal bounderanes inroughout

Cheriy Urroughout

Flubtite Predum ates above 170in

and sulphides helow (Oi

Berumindus oratetial in laminae and 4tylatiles

ia 329 60m

1 et

Fig. - Simplified log, Maria 1-B, Officer Basin.

‘

EARLY CAMBRIAN TRILOBITES FROM OFFICER BASIN 199

Fig. 4. A. P22981, immature cranidium, X9. B.

P22982, part of left hand anterior part of crani-

dium, X8. C. P22983, partial cranidium, X7.5.

All photographs are of silicone rubber casts

whitened with magnesium oxide.

The other two specimens, P22982-3 (Figs

4B-C), represent a single species. This species

has a glabella which apparently has a well

developed occipital furrow and three pairs of

lateral glabellar furrows. The lateral glabellar

furrows are directed inwards and backwards,

with the anterior furrows being shallower than

the posterior furrows. The position of the

glabellar anterior cannot be determined. The

wide palpebral lobes extend from opposite the

occipital furrow to opposite the 3p glabellar

furrows; the wide eye ridges meet the glabella

immediately forward of the 3p glabellar fur-

rows, There is a suggestion of the presence of

a para-frontal band.

The wide, almost flat border widens

abaxially; it stands well above the preglabellar

tions of the facial suture commence opposite

the 3p furrows and diverge markedly to the

marginal furrow, from where they converge

gently. The almost flat palpebral areas of the

fixigenae are separated from the palpebral

lobes by narrow shallow furrows.

The short, postocular sections of the facial

sutures diverge markedly and enclose small

posterolateral limbs. The marginal furrows are

broad. The forward part of the glabella has a

low reticulate ornament. The remainder of the

cranidium visible is finely granulose.

The shape of the facial suture, and the shape

and position of the palpebral lobes suggest

affinity with Pararedlichia, Eoredlichia, Wutin-

gaspis, Chaoaspis or a related genus of the

Redlichiidae. Such genera are found in lower

Lower Cambrian rocks of China (Chang 1966,

Lu et al. 1974, Li 1980), France (Courtessole

& Jago 1980), Vietnam and Morocco (Hupé

1953). In South Australia Eoredlichia has been

recorded from Faunal Assemblage II in the

Flinders Ranges (Daily 1972). Daily cor-

related this assemblage with the early part of

the Atdabanian of Siberia, This suggests that

the specimens figured herein are also of early

Early Cambrian age. However, until more

material is available a more precise age cannot

be given, The presence of further trilobite

fragments at a depth of 333 m in Marla 1B

indicate that the fauna figured herein cannot

be of earliest Early Cambrian age.

Acknowledgments

B. C. Youngs publishes with the permission

of the Director-General, S.A. Department of

Mines and Energy. Dr B. Daily (University of

field from which it is separated by a narrow, Adelaide) is thanked for useful advice and

shallow marginal furrow. The preocular sec- criticism.

References

Cuana, W. T. (1966) On the classification of Red-

lichiacea, with description of new families and

new genera. Acta Palaeont. Sinica 14, 135-184

[Chinese].

CourtTEssoLe, R. & Jaco, J. B. (1980) Biostrati-

graphie du Cambrien inférieur du Cabardes

(versant sud de la Montagne Noire, France

méridionale. Geobios 13 (in press).

Daity, B. (1972) The base of the Cambrian and

the first Cambrian faunas. Univ. Adelaide

Centre for Precambrian Res. Spec. Pap. 1, 13-

42.

GateHouse, C. (1976) A fossil in the Observatory

Hill Beds, South Australia. Quart. geol. Notes,

Geol. Surv. S. Aust. 60, 5-8.

Hupé, P. (1953) Contribution a l'étude du Cam-

brien inferieur et du Précambrien III de l’Anti-

Atlas marocain. Notes Mém. Serv. Geol. Maroc,

103, 402 pp.

Lt, S. J. (1980) Trilobites from the Chiulaotung

Formation (Lower Cambrian) in Emei Area,

Western Sichuan. Acta Palaeont. Sinica 19, 42-

50 [Chinese].

Lu, Y. H., Cuu, C. L., Curren, Y. Y., Lin, H. L.,

Cuow, T. Y. & Yuan, K. S. (1974) Bio-environ-

mental control hypothesis and its application to

the Cambrian biostratigraphy and palaeozoogeo-

graphy. Nanking Inst. Geol. Palaeontol. Mem.

5, 27-110 [Chinese].

Pitt, G. M., Bensow, M. C. & Younes, B. C.

(1980) A review of recent geological work in

the Officer Basin, South Australia. J. Aust.

Petrol. Explor. Assoc. 20, 209-220.

THoRNTON, R. C. N. (1978) The geological results

of the drilling of Manya No. 1 and Marla No. 1.

Miner, Resour. Rey. S. Aust. 143, 47-65.

Wuite, A. H, & Younas, B. C. (1980) Cambrian

alkali playa lacustrine sequence in the north-

eastern Officer Basin, South Australia. J. Sed.

Petrol. (in press).

MUCKERA AND MILLBILLILLIE —- AUSTRALIAN ACHONDRITIC

METEORITES

BY M. J. FITZGERALD

Summary

The chemistry, mineralogy and petrographic features of two Australian achondritic meteorites are

described in detail. The previously undescribed South Australian meteorite, Muckera, found on the

Nullabor Plain in 1951, is classified as a howardite. One of the masses of the Millbillillie meteorite

from central Western Australia is shown to be chemically and mineralogically similar to another

mass presumably from the same fall. This new mass is classified as an eucrite.

MUCKERA AND MILLBILLILLIE—AUSTRALIAN ACHONDRITIC

METEORITES

by M. J. Firzcnracn*

Summary

Erezoeraco, M. J, (1980) Mueckera and Millbillitiie—Australian achondritie meteorites. Trams.

R. Sac. S. Aust, 04(6), 201-209, 28 November, 1980,

The chemistry, minernlogy and petrographic features of two Australian achondritic

meteorites are described in detail, The previously undescribed South Australian meteorite.

Muckera, found on the Nullarbor Plain in 1951, is Classified as a howardite. One of the masses

of the Millbillillie meteorile from central Western Australia is shown to be chemically and

mineralogically similar to another mass presumably from the same fall. This new mass i¥

classified 65 an euerite.

Introduction

Meteorites can readily he subdivided into

two groups on the basis of bulk chemistry,

with the individuals of one group having

compositions resembling the sun. These undif-

ferentiated meteorites are known as chandrites

as most contain chondrules—small spheroidal

bodies commonly having diameters of the

order of one millimetre which typically contain

varying amounts of erystalline material in

dendritic or skeletal form, and glass, which

may Or may not be devitrified. Of the three

major chondrite groups — carbonaceous,

enstatite and ordinary—the carbonaceous

chondrites. best approximate pristine solar

material even though they have undergone

some alteration, albeit isochemical (McSween

1979).

Conversely, an achandrite is a meteorite

whose chemisity is unlike that of the sun.

Traditionally this term has been restricted to

differentiated meteorites containing little or to

free metal, but this restriction appears ta

conceal important genetic relationships,

The differentiated and undifferentiated

meteorites can be distinguished on the basis of

their chemistries relative to the Cl (type i

carbonaceous) chondrites by cvaluating the

following ralios (atomic abundances nor

malized to 100 silican atoms):

K/0.42, Al/8.5, Ca/ 7.21, P/0.96, Ti/0,2775

and Fe/83.0

with the divisors being the corresponding

normalized abundances for the C1 chondrites

from Cameron (1973), An undifferentiated

meteorite is then ucfined as one for which

these ratios generally fall in the range 0.4 to

1.3 while the achondrites fall outside,

Centre for Precambrian Research, University of

Adehode, G.P.O, Box 498, Adelaide S007.

The achondrites can be subdivided into nine

eroups on the basis of selected atomic ratios

(on a percentage basis) with almost every

member of two of the groups, the eucrites and

howardites, being characterized as follows:

Eucrites Howardites

AV/Si S10

Fe/5i <= 100

Ca/Si > 20 <20

These two groups encompass a large pro-

portion of the silicate-rich achondntes and

because of their chemistry and mineralogy

are often collectively referred to as the basaltic

achondrites, They consist essentially of plagio-

clase and pyroxene with pigeouite generally

predominating in the euerites and hypersthene

in the howardites. This predominance of

calcium-rich pyroxene im the eucrites is

reflected in the Ca/Si ratio used to charac-

terize them,

Most of the ecuerites and howardites are

breceiated with the former being deseribed as

manomict breccias (tc. they contain clasts

Which are similar in composition), although

some of these meteorites show little evidence

of brecciation, On the other hand = the

howardiles, almost without exception, contain

clasts which vary widely in texture and com-

position but which nonetheless appear to be

closely related to cach other and are thus

deserlbed as polymict breccias (cf, Duke &

Silver 1967, Wasson 1974, Mason er al. 1979).

The basaltic achondrites resemble breceiated

materials recovered from the lunar surface

and it is likely that all are surface breccias

produced by similar processes.

These chemical and petrological definitions

are generally complementary and in most cases

produce a consistent classification, However,

there seems to be a genetic relationship

202

between the two proups which renders the

distinction between them somewhat unneces-

sary, Furthermore, this relationship extends

to other achondrite groups as presently defined

and it ts suggested that they should all be

grouped together under the generie heading

of “cognate achondrites”.

Muckera Meteorite

Mistavical Background

On either May 1 or 2, 1951, while walking

some 3 km SW of a group of rock holes on

the northern edge of the Nullabor Plain about

70 km north of Cook and known as Muckers

Rock Hole (30°05'S 130°02’E), Police Con-

stable C, P, Doyle kicked a rock and. as it

seemed different from the country rock, picked

it up. Mr Doyle removed much of the cover-

ing crust in an attempt to identify the abnor-

mally heavy rock but was not successful and

so took it back to Cook. Ultimately the

meteorite Was brought to the Geology Depart-

ment of the University of Adelaide in Feh-

ruary 1972 where it was identified as a

meteorite hy Dr J. B, Jones, The meteorite

was named Muckera. This hame is sufficiently

different from Mukerop, a rarely used synouym

for the Giheon meteorite, to avoid confusion,

This is the first published account of the

Muckera meteorite other than the author's

classification given by Hutchinson er al.

(1977) and mentioned by Mason et al.

(1979).

Deveription

The meteorite is approximately ellipsoidal

in shape (Fig. |), and about 10 * 8 ® 5 em.

Part of the fusion crust which is commanly

red-brown in colour due to terrestrial weather-

ing is still preserved. This crust also contains

occasional white mineral grains.

Internally the meteorite consists of sub-

rounded to angular fragments, varying 01-3

cm. set in a dark grey to black eroundmass,

Small grains of fickel-iron and troilite, sur-

rounded in mast cases hy weathering haloes,

ure present. Commonly the nickel-iron is

confined to the clasts, while the dark colour

of the matrix is due to the presence of fine-

grained tarnished sulfides and olass. Oliyine

and calcium-rich pyroxenes are generally con-

fined) to the dark matrix whereas most of the

M. §, FITZGERALD

calcium-poor pyroxencs are in the clasts.

Numerous fractures and vughs, many of which

are lined with, and commonly filled by, a

brown mineral, ace present. In same cases

this filling is layered parallel to the cavity

walls.

Many of the silicate clasts are white to

cream. others are colourless. Many are aggre-

gates of smaller, sub-rounded clasts which in

turn are composed of angular and sub-rounded

mineral fragments (Fig, 2),

Petrographie examination emphasises. the

brecciated nature of the meteorite (Fig, 3).

The grotindmass, containing abundant glass,

is dark grey to black while the fragments are

eammonly light grey. Several different types of

clast are present, ranging from mimeral frag-

ments through monomineralic aggregates ta

polymineralic lithic clasts,

The monominerali¢c fragments include both

angular pyroxene and Jarge plagioclase prains,

many of which are strongly shocked and

braken but not disaggregated. The rmono-

mineralic aggregates include fragments. which

in terrestrial racks would be referred to as

orthopyroxeniles and anorthosites,

The lithic fragments include rock types such

as hasalts as well as numerous fine, equi-

granular breceia clasts containing angular

to sub-rounded grains, Pyroxene is more

abundant than feldspar in these pre-existing

breccias anda plassy mesostysis is commonly

present. There is generally littie miatris

material separatiny the small clasts whiely have

been Incorporated into the larger ones.

Muekera is thus a palymict breecia with a

clast to matrix ratio of about S:1, the latter

being composed nainly of glass and small

grains exhibiting a wide variation in grain size

and composition. Such textures can be readily

imagined as having been produced by repeated

impacts on the surface layers of the meteorite

parent body so producing fragmental material

which was subsequently compacted and

lithitied.

Milthillitlie Meteorite

Historical Background

At about | p.m, one day in October 1960,

Messrs F. Quadrie and F. Vicenti, two stution

hands working near the boundary fence

Om. re 8

Fig. |, External view of Muckera meteorite: Absence of fusion crust reveals Ir@mental nitive of

meleoriie, Scale 2 cm,

Fig. 2, Polished slab of Muckera meteorite showing brecciated texture. Scale | em

Fiy. 3. Thin section of Muckera meteorile showine diverse nature of clasts, Seale 2 mr.

ILLIE METEORITES 203

-RA AND MILLBILL

CKEI

204 M. J.

Fig. 4. External surface of Millbillillie No. 3

meteorite showing fusion crust and radiating

bubble trains, Scale 2 cm.

between Millbillillie and Jundee Stations in

the Wiluna district, central W.A. (26°27’S

120°22’E), saw a fiery object trailing sparks

fall on a spinifex-covered area of the plain

to the north. No search was made but Mr D.

Vicenti found a piece of meteorite on the

plain in 1970. This mass weighed about 20 kg;

another mass of some 600g was found the

next year by Mr M., Finch (Clarke 1972).

Further material has been recovered in the

area by local aborigines. The third recorded

recovery was purchased by the late Mr Clem

Latz of Adelaide thereby precluding its export

from this country. This 368g individual was

completely covered with a fusion crust when

purchased, and from it a mass of some 26g was

acquired by the University of Adelaide. A

portion of this mass was used for the analyses

described in this paper. Subsequently, the

main mass of 233g was also acquired by the

University. The designation No. 3 was

appended to this mass to indicate that it is

the third documented recovery from the area

(cf. Graham 1980).

Oher specimens of the meteorite include

those lodged in Museums in Perth, Sydney,

Canberra and London and in private collec-

FITZGERALD

tions in Wiluna. All told it appears that at

least 26 kg of material has been recovered.

Some results have been reported for the

first mass found, Passing references to its

petrography were made by McCall (1973)

and several trace elements have been

determined (De Laeter & Hosie 1978; McCul-

loch et al. 1976, 1977; Rosman & De Laeter

1978; and Smith et al. 1977). At least two

bulk analyses have been carried out—one by

Dr J. A. Nelen (Mason et al. 1979), and

another by Dr R. A. Binns (Stolper 1977)

which is yet to be published in full, This

paper presents the first published results for

the third mass.

Description

The No. 3 mass resembles a flattened

ellipsoid with dimensions about 4 X 7 X 10

cm (Fig. 4). It is completely encrusted with

a black glassy layer about 0.3 mm_ thick

underlain in turn by dark crystalline material

and a further layer of a light coloured crystal-

line material. Much of the crust, which is

patterned with numerous lines radiating from

a central point on one of the flat surfaces,

is now covered with an orange film. The sur-

face lines consist of trains of numerous dark

brown to black glassy bubbles about 0.5 mm

in diameter; other bubbles are randomly

distributed over the remainder of the crust.

Furthermore, the crust exhibits a series of

polygonal fractures commonly forming quad-

rilaterals with dimensions about 2-5 mm. The

individual cracks are less than 0.1 mm wide

and are filled with the orange material which

covers part of the crust surface. In places

this filling stands above the level of the

surface and in other cases below. In general,

the fractures do not extend through the

fusion crust. However, in rare examples where

the fractures do pass through the crust, the

secondary orange mineral occurs along the

interface between the crust and the interior

mass of the meteorite. In some places the

orange mineral is, in its turn, overgrown with

an apple-green one.

A cut surface shows numerous sub-angular

particles from 0.1—3 cm set in a grey to white

crystalline matrix, A sub-ophitic texture can

be seen in some of the coarser-grained clasts

even at low magnification. Clast-rich and clast-

poor regions define a layering. Finer-grained

clasts generally possess very sharp boundaries

whereas the coarser ones commonly merge into

the matrix, the grain size of which increases

in that area, resulting in the average grain size

MUCKERA AND MILLBILLILLIE METEORITES

of the clast-rich regions being greater than

that of the clast-poor regions. No metal or

sulfide grains were seen on the surfaces

examined,

The two clast types are readily seen in thin

section (Fig. 5). The finer consist of extremely

fine-grained granoblastic aggregates contain-

ing many opaque grains while the coarser

clasts are ophitic and subophitic basalts, that

is, feldspar and pyroxene aggregates. The feld-

spar laths in these basaltic areas vary in

length up to 0.5 mm while occasional equi-

dimensional grains achieve similar dimensions.

In addition to these clasts there are also

numerous feldspar fragments and spherulitic

aggregates of devitrified glass. The silicate

grains contain numerous opaque inclusions.

The merging of the coarse-grained clasts and

matrix is even more obvious in thin section

and some of the matrix is also basaltic in

205

texture. The layering seen on the macro scale

can also be seen in thin section. There is no

evidence of brecciation either within the

basaltic clasts or in the host matrix,

The matrix consists of tiny (0.02—0.03 mm)

grains of pyroxene and feldspar set in glass

with an overall texture of “feathery” quench

material. Much of the matrix has been devitri-

fied and recrystallized. There is no evidence of

weathering in the form of iron-staining but

the matrix appears dark due to the presence

of numerous grains of opaque minerals and

regions of opaque glass.

It is concluded that the fine-grained clasts

may have been incorporated into the matrix

prior to crystallization. There are several

ways of achieving this—one possibility is that

pre-existing clasts (possibly impact-derived

fragments of a rapidly cooled lava flow) were

caught up in a later flow which _ initially

cooled less rapidly perhaps as a more extensive

lava flow or blanket. During this cooling stage,

gravitational setting could have brought about

the layering. Subsequent rapid crystallization

arising from changes in the cooling regime or

the attainment of conditions of supersatura-

tion in the liquid phase could have produced

the glass in the matrix. Regardless of the exact

mode of formation of the texture, subsequent

shock events must have been minimal as any

such — significant reworking would have

destroyed this layering.

Bulk chemical compositions

X-ray fluorescence analysis was used for

the determination of all elements except

sodium for which a flame photometric

method was employed. A modified version of

the Norrish & Hutton (1969) technique for

XRF analysis was used. Mineral compositions

were determined with a Technisch Physiche

Dienst microprobe fitted with a lithium drifted

silicon detector, the method of Reed & Ware

(1975) being used to reduce the data, Full

details of all methods are given in Fitzgerald

(1979).

The bulk chemical compositions of the

meteorites are listed in Table 1 along with the

results of normative mineral calculations. The

assumptions made in the modified form of

the CIPW calculations used to calculate the

norm are fully explained in Fitzgerald (1979).

Phosphorus has been allocated to the mineral

merrillite, (@-Ca,(PO).), as Dowty (1977)

has shown this is the principal meteoritic

phosphate. For comparative purposes, Table 2

also lists the results of Mason ef al. (1979).

206

TABLE |, Buelk chemical composition and narmative

minerqlogy.

Elemental

abundances

(weight Millbillillie Millbillillie

percent) Muckera! No. 3! No, 1

Fe 13.85 15,30 14.22

Mn 0.40 0.46 O47

Ti 0.25 0.44 (4)

Ca 5.06 7.42 7.29

K 0.040 0.071

P 0.029 O.034

Si 23.20 23,84 24,3]

Al 4,32 7,03 6.77

Mg 8.95 4.42 4.05

Ni 0.090 0.018

S 0.27 0,003

Cy 0.37 (21 0,23

Na (2) (33 0.29

Normative

mineralogy

(weight percent)

Nickel-iron ().7 0.4

Troilite 0,7 0.01

Merrillite 0.1 0,2

[lmennte 0.8 3

Chromite O# O4

Feldspar 23.9 34.3

Diopside 1S 13.0

Orthopyroxene 67.0) 41.9

Olivine as

Quartz 8.9

Molar percent

composition

Ah 11 It

An 88 88

Ps 35 40

Fa 3

tT his work *Masan etal. (1979)

As Mason (1962) pointed out, there is an

almost perfect balance between silica and the

basic oxides in the basalGe achondrites so

that a slight excess results in quartz being

present or a slight deficit appears as olivine.

The excess silica generally occurs in the

eucrites and the olivine in the howardites, The

normative caleulations of Table 1 jlustrate this.

Mineralogy

Eucrite and howardite fteldspars commonly

fall in the compositional range Any, o9;. with

most compositions lying in the narrower range

Angs-an (Duke & Silver 1967). Feldspar

compositions measured in this work (Table 2)

lic within these limits and are accordingly

consistent With the classifications proposed

below

M. J. FITZGERALD

The pyroxene Variation in Muckera (Fig, 6)

is very similar to that of the Kapoeta and

Malvern howardites (Desnoyers & Jerome

1977; Duke & Silver 1967; Dymek ef al.

1976; Simpson 1975), The majority of the

analyses fall within the field En, Fs. ,-Eny ,,

sz y—Eny 4 F854, Woo Eng yFsyq Won, This

Variation is in distinct contrast to that of the

eucriles.

In these cases Duke & Silver (1967) found

a continuous range in composition from

pigeonite through sub-calcic ferroaugite to

ferroaugite with the magnesium silicate com-

ponent remainifig relatively constant, Figure

7 shows such a situation for Millbillillie and,

exeept that the most calcium-rich analyses

show about 5 mole percent more of the

calcium silicate component than the results of

Duke & Silver, the distribution most closely

resembles that of Juvinas as figured by these

authors. A more fecent determination

(Takeda et al. 1978) shows an even closer

resemblance between Juvinas and Millbillillic.

The Millbilllilie results are also yery similar

fo those obtained by Desnoyers & Jerome

(1977) for a clast in the Malvern howardite.

Simpson (1975) and also Wilkening & Anders

(1975) have suggested that this apparent

linear series of compositions, which is charac-

teristic of eucritic pyroxenes, results from the

analysis of differing proportions of two

exsolyed phases, the lamellae being too fine to

resolve with the microprobe. Mason ef al,

(1979) came to a similar conclusion, Micron

sized lamellae visible in many of the Millbil-

lillie pyroxene grains are probably thus

responsible for the trend seen in Figure ‘7.

Modal olivine was not observed in Millbil-

lillie und miner amounts only in Muekera, In

the latter it was confined almost exclusively

to the dark groundmass with only uo few

prains being found in lighter clasts, The com-

TABLE 2. Mineralogical comiposilions,

ML i ay

Muckeru! No, 3! No

Feldspar

(% An)

Runge T4 lo 04 78 lo 2 &2to4l

Average 88 84 Ra

Pyroxene —_— Fisuo Wax Fsiy Won

lo, to

Fsoy Woy, san Woy

‘This work *Mason ef al, (1979)

MUCKERA AND MILLBILLILLIE METFORITES 207

rad —

Shs

Fig, 6. Pyroxene compositions in Muckera meteor-

ite,

f m An

“ \

neal a. .

Fig. 7. Pyroxene compositions in’ Millbillillie No.

3 meteorite.

positional range Fasy 95, as measured by

microprobe, is consistent with the results of

Desnoyers & Jerome (1973). These modal

results are in accord with the normative calcu-

lations of Table 1.

The iron-manganese correlation in lunar,

meteoritic and terrestial olivines and pyroxenes

is well documented with the three groups

being fairly readily distinguished on this basis

(Desnoyers & Jerome 1973; Dymek et al.

1976; Simkin & Smith 1970). The correlation

arises as a result of the ability of Mn*+ to

replace Fe+* in olivine and pyroxene lattices

due to the similarity of their ionic radii

(Wanke et a/, 1973). Intergrain constancy of

this ratio indicates the grains have been

derived from related source materials (Dymek

et al. 1976).

The Muckera pyroxenes and olivines show a

wide range in iron and manganese contents.

That the pyroxene data is somewhat non-

cohesive is shown by the correlation coefficient

of 0.91 for 118 determinations, The average

Fe/Mn ratio for the pyroxenes is 28.8, while

the value for the bulk analysis is 33.9 (Fig. 8).

A relatively narrow range in iron composi-

tion in the olivine, coupled with a considerable

spread in manganese values, results in the

relationship between these elements in the

olivine grains being less obvious (Fig. 8), with

the spread being indicated by the lower cor-

relation coefficient of 0.34 for the 50 analyses,

The average value of the ratio for the olivine

is 50.3, thereby explaining the difference

between the bulk ratio and that of the

pyroxenes.

In Millbillillie the pyroxenes also exhibit

a wide range in Fe and Mn values but the

data is even more cohesive as shown by the

correlation coefficient of 0.97 for the 103

analyses (Fig. 9). The value of the ratio for

the bulk analysis ts 33.1 while the average

value for the pyroxene analyses is 32.9. Simi-

lar agreement of pyroxene and bulk chemistry

is shown by eucrites such as Moama (Lover-

ing 1975) which has a bulk ratio of 29,3 and

one of 27.5 for the host hypersthene.

Classification

Table 3, giving values for several atomic

ratios discussed previously, clearly shows that

both Muckera and Millbillillie are differen-

tiated meteorites while Table 4 shows that,

on the basis of the ratios listed here, Muckera

is a howardite and Millbillillie an eucrite,

Feldspar, pyroxene and olivine contents and

compositions are consistent with these classi-

fications as are the petrological descriptions

showing Muckera to be a polymict breccia

and Millbillillie monomict. Muckera is thus

L 7 —

= 0

reo

Fig. 8. Plot of MnO versus FeO in Muckera

meteorite olivines und pyroxenes. X: bulk com-

position,

7] red 3

Fig. 9, Plot of MnO versus FeO in Millbillillie No.

3 meteorite pyroxenes. X: bulk composition.

208

Tasre 3. Evaluation of “differentiation” ratios on

atomic hasis.

Ti’

K/0.42 AWS Cal7-2b P/0.96 0.2775 Fe/83 0

RA eT oil 2 D4

Millbil-

lillie No.3 05 36 3.0 Of 39 D4

TABLE 4. Classifications based on atomic ratios

(an a percentage hasis),

_ Ratios Classilica-

AL/Si Fe/Si- Cu/Si tion

Muckera 19.4 30,2 15.3 Howardite

Millbillillic

No. 3 30.6 32.4 21.8 Fuerite

the first recorded example of a polymict brec-

ciated achondritic meteorite to be recovered

in Australia,

M. J. FIIZGERALD

On the basis of chemical and textural fea-

tures it has been suggested (c.g. Stolper 1977)

that most of the known eucrites lie together

in a cohesive group with the others in iwo

smaller groups with one containing eucrites

deseribed ay cumulates and the other meteorites

considered to be residual fractions. Applica-

hon of the technique of Principal Component

Analysis by the author (Fitzgerald 1979)

to a data set including analyses of 32 eucrites

has shown that Millbillillig belonys to the

main body of the cucrites, an assignment

Which is supported by the textural relation-

ships described above.

Acknowledgments

This work was carried out during the tenure

of a University of Adelaide Postgraduate

Research Grant and the receipt of both this

and the constructive help wad criticism of Dr

J. B. Jones and an anonymous referee is

gratefully acknowledged,

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