VOL. 91 DECEMBER, 1967
TRANSACTIONS OF
THE ROYAL SOCIETY
OF SOUTH AUSTRALIA
INCORPORATED
ADELAIDE
PUBLISHED AND SOLD AT THE SOCIETY'S ROOMS
KINTORE AVENUE, ADELAIDE
Price: Six Dollars Thirty Cents
A REVISION OF THE STARFISH GENUS UNIOPHORA
(ASTEROIDEA; ASTERITDAE)
BY S. A. SHEPHERD*
Summary
The genus Uniophora which is widely distributed in temperate Australian seas is reviewed.
Uniophora globifera, U. fungifera, U. sinusoida, U. multispina, U. obesa, U. uniserialis are placed
in the synonymy of U. granifera, and U. gymnonota is considered to be a synonym of U. nuda.
Population samples from Spencer and St. Vincent Gulfs, South Australia, are analysed and
statistical differences noted. Specimens from New South Wales, Victoria and Tasmania are
compared and observations are made upon the ecology and distribution of the South Australian
forms.
A REVISION OF THE STARFISH GENUS UNIOPHORA
(Asteroidea; Asteriidae)
by S, A. SHerpHEeRD®
[Read 14 July 1966]
SUMMARY
The genus Uniophora which is widely distributed in temperate Australian
seas is reviewed, Untophora globifera, U. fungifera, U. sinusoida, U. multiypina,
U. obesa, U. uniserialiy are placed in the synonymy of U. granifera, and U.
Eymnonota is considered to be a synonym of U, nuda. Population samples from
Spencer and St. Vincent Gulfs, South Anstralia, are analysed and. statistical
differences noted, Specimens from New South Wales, Victoria and Tasmania
are compared and observations are made upon the ecology and distribution of
the South Australian forms.
INTRODUCTION
The genus Uniophora is a prominent and distinctive representative of the
seastars of temperate Australian waters having a distribution around the coast
of the southerly half of the continent from Collaray Reef near Sydney on the
east coast to Lancelin Island in Western Australia,
The members of the genus are extremely variable and have long been a
source of perplexity to taxonomists. Lamarck (1816) described Asterias grani-
fera from Tasmania and Gray (1841) created the genus Uniophora naming U,
globifera from New South Wales. Perrier (1875) described Asterias nuda from
Pt. Lincoln, South Australia, Asterias fungifera from “Nouvelle Hollande” and
Asterias sinusoida from Hobart, Tasmania. The species of Lamarck and Perrier
were all subsequently placed in the genus Uniophora. In 1923 Clark added U.
dyscrita from Western Australia and in 1928 U. gymmnonota, U. muitispina,
U. obesa and U, wniserialis all from Spencer or St. Vincent Gulfs, South Aus-
tralia. Subsequent shore collecting (Cotton and Godfrey, 1942) showed that
of the ten species, certainly eight and probably nine were to be found in the
gulfs of South Australia.
This paper is largely the result of collecting by the author with SCUBA
diving apparatus over a number of years. The examination of the considerable
material so gathered shows that the supposed speciation of the genus in the
South Australian gulfs does not exist, and it is believed that there are only two
species in South Australian seas.
The collections of the Australian Museum, the National Museum of Victoria
and the Western Australian Museum have been examined; the forms from
Victoria, New South Wales and Tasmania are vonsidered conspecific with
U. granifera but the Western Australian form U. dyscrita is regarded as specific-
ally distinct. Differences between the several forms are discussed and spine
*c/- South Australian Museum, North Terrace, Adelaide, South Australia.
Trans. Roy. Soc. §. Aust, (1967), Vol. 91,
& 5S, A. SHEPHERD
counts are used lo determine statistical differences between population samples.
This method is belicyed to be noyel in the study of astervids. Geographical and
ecological notes are also given and a map showing the distributions of the
various forms in the gulf regions is added,
In this paper the following abbreviations are used; A.M., Australian Musemm;
N.M.Y., National Museum of Victoria; S.A.M., South Australian Museum.
W.A.M,, Western Australian Museum,
UNIOPHORA GRANIFERA Lamarck
Asterias granifera Lamarck, 1516, p, 560,
Uniophora globifera Gray, 1840, p, 288,
Astevias fungifera Perrier, 1875, p. 337,
Asterias sinusoida Perrier, 1875, p. 338.
Uniophora sinusoida Clark, 1928, p. 411.
Uniophora obesa Clark, 1928, p. 409,
Uniophora uniserialis Clark, 1928, p. 415.
Uniophora. multispina Clark, 1928, p, 407.
Uniophora multispina multispina Stach, 1938, p. 832.
Uniophora multispina uniserialis Stach, 1938, p. 332,
Material Examined, “Granifera” group. S.A.M. (117 specimens) KI174-6,
K191, K597-8, K600, K629-K641. A.M. (16 specimens) from N.S,W. ].127-8,
J.l44, J.7444, J.6884, ],7008. From Tas, J141, J.143, |.168-9, ].5410-5414.
N.M.V., 5 specimens labelled Port Phillip Survey, “Multispina” yroup (98 speei-
tnens) S.A.M. K181-38, KI85, K187-9, KI90, KI93. K520-1, R601-2, K605, K626,
K635, K643-651.
In 1875 Perrier (1875, p. 342) noted the puzzling diversity of the specimens
befure him and considered them to comprise four distinet species. Later Fisher
(1923, p. 597) referred Gray's. globifera to the species granifera. Tt is now clear
that there is only one species which shows considerable morphological variation
both between and within its component populations. The differences in mor-
pholowy relate principally to the frequency, size and regularity of arrangement of
the dorsal spines. The populations examined fall into two groups cach of which
has its own preferred habitat and. finds a distinctive phenotypic expression. One
group is called “granifera” as specimens of it have predominantly the chariac-
teristics. formerly ascribed to U. granifera and the other group is termed “multi-
spina” to indicate a similar relationship with the former species U, mudtispina,
“Granifera” Group
This group is polymoerphic and falls into three more or less couspicuuns
forms. Ifistorically these forms have been treated as three species, namely,
Uniphora granifera, U. sinusolda and U. fungifera. A given population of the
eroup may contain representatives of all three forms but usually there is a
preponderance of one form with a few representatives of one or both of the
other forms. Where two of the forms. are represented in a population there
are usually numbers of specimens of intermediate form, and on ocvasions speci-
mens of one form have heen seen with a regenerated arm of another form,
The form first deseribed as U. globifera is most commonly enconntcred anil
is characterised by swollen and capitate carinal spines. A typical specimen is
figured by Clark (1923, p, 404). The carinal series of plates carries np te 24
enlarged capitate spines, frequently placed singly at the apex of each zizzug
formed by the outline of the plates. Interspersed between these enlarged spines
are a variable number of much smaller capitate spines either singly or in small
“tiups. The dorso-lateral plates have numerous spines of varying size usually
“ REVISION OF “VHE STARFISH GENUS UAIOPHOHA a
about as large as the smaller spines of the carinal series and these ave often
irregularly placed. Here and there the spines of the superd-marginal plates
are as large as thase along the carinal lines.
Specimens from New South Wales which have this form are remarkable [or
the size of their enlarged capitate carinal spines which are larger than thase seen
in South Australian specimens. They also differ from the latter in possessing a
larger number of smaller capitate spinelets dorsally and on the intermaryinal
plates, The actino-lateral spines are quite variable; sometimes they are typical
but at others more like those in “multispina” group. The specimens were all
taken apparently on rocky bottoms and are cither from Long Reef, Collaroy, or
Sydney Iarbour.
A second form which was formerly designated U. sinusvida possesses a
markedly zigzag carinal scries of plates bearing spines which are capitate but not
nearly as conspicuous as the globose spines of the previous form, In some
specimens it is dificult to detect a carinal series of plates at all and dorsally the
spines appear to form the margins of a series of discontinuous polygonal papular
areas. The figures of Clurk (1928, p, 412) and Stach (1938, p. 332) are quite
typical of this kind of specimen.
A number of such specimens haye been examined from Port Phillip Bay,
Victoria and have less conspicuous dorsal spines than the South Anstralian
specimens while several rather resemble those in “multispina” group, Specimens
from the Austvalian Museum taken in Tasmania are placed in this group with
sume hesitation, The arrangement of the spines awd the general appearance of
these specimens are typically sinuyoida-like but the dorsal spines of some speci-
mens, particularly those taken in 1)’Entrecasteanx Channel, Tasmania, are fine and
pointed as is sometimes the case in “multispina” group,
ly same localities there commonly appears a third form which is remurkable
for the proliferation of spines dorsally. Instead of enlarged capitate spines
aceurring, singly or in groups of two or three along the carinal series, there are
groups of 10 to 20 small and closely appressed, capilate spines, often with the
central cue much larger than the surrounding ones. These groups of spines are
usually contiguous. and together appear to form am almost Hat dorsal surface.
In othey respects the specimens do not differ significantly from those previously
mentioned, These specimens conform to such » striking degree with Perrier’s
deseription of Asterias fungifera (1875) that nv doubt this form, or somethrig
very close to it, is that which is so described. Jt is to be nated also that Fisher
(1926, p, 198) who compared the type specimens of Asterias fungifera and
Asterias yinusoida thought the Jatter to he a “slenderer and stouter spined
exantple of the same species”,
1! have only ohserved “granitera” populations an reels and rocky bottor,
Stach (1938) however, reports several specimens from Posidonia beds in the Sir
Joseph Banks Croup, Spencer Gulf, South Australia, but it is possible that these
specimens came froma granitic reef nearby, Some of the specimens from Port
Phillip Bay, Victoria, and also from D’Entrecasteaux Channel, Tasmania, alsu
appear to occur on sandy bottom but as indicated previously these specimens are
atypical. The form ranges fram lnw water down to about 20 m in depth but is
found in greatest wbundance in depths between 5 and 10 m; in fayourable con-
ditions where the wave action is moderate but not severe two or three specimens
may oceur to the square metre,
The favourite dict is a small tunicate which abounds on shallow reefs.
Very frequently the seastar is found with its rays encircling the Uinivate and
6 &. A. SHEPHERD
protuding its everted stomach into the animal's oral aperture. low it achieves
this is not known. Its tube feet clearly could not exert the same foree on the
tunicate as they could upon the shells of a bivalve. In the latter case the force
exerted by each tube-foot on the shell would be cumulative; whereas in the
former case, the aperture appears to be controlled by musculature immediately
surponn alg it and the seastar could bring very few of its tube feet to bear upon
these muscles, and hence would exert little farce on them, It is possible that the
animal discharges a stomach enzyme or toxin which paralyses or narcotizes its
prey so enabling it to vain entry, Certainly when the starfish is removed the
tunicate is unusually sluggish in closing its aperture. To a lesser degree the
seastar has been observed toa feed on reef-dwelling univalves and bivalves and
on various encrusting ascidians, Specimens taken from shallow water are usually
brick-red in colour but occasional ones are seen in which the papular areas are
a dark blue. Specimens from deeper water between 15 and 20 m are usually
more brightly coloured, ranging from bright red to orange. Orally specimens are
red to orange.
“Multispina” Group
Specimens from thesé populations are distinguishable from those of “yrani-
fera” Populations by the comparatively regular arrangement of the carinal and
dorse-lateral plates and the spines on them. The carinal series carries from | to
4 rather small capitate spines to each plate and the series forms a straight linc
medially on the dorsal surface with a tendency in some specimens to zigzag
distally. On each side of this series and parallel with it are two regular dorso-
lateral series carrying similar but smaller spines. In some populations the latter
series bear spines only sporadically and the sipero-marginal series bear them
ieguiarly, The spines themselves vary considerably from being capitate or
bluntly pointed to being fine and sharp. Where “multispina” and “granifera”
populations intergrade, as is not uncommonly the case, the characteristic dif-
ferences tend to become obscured,
The forms described by Clark as U. obesa and U, uniserivlis are beth well
within the range of variability shown by “multispina” races and there can be no
doubt as to their synonymy. The figures of Clark (1928, pp. 407, 410 and 412)
indicate the remarkable diversity existing in the appearance of specimens.
“Multispina” populations are abundant on the angiosperm beds of Cyma-
docie antarctica Endlicher, Posidonia australis Hooker, and Zostera mueller
Irmisch characteristic of the coastal margins of the South Australian Gulfs par-
ticularly in the less exposed regions. ‘Their principal diet is bivalves and uni-
valves which are abundant in the sand among the fibrous angiosperm roots.
Mast specimens are dark red in colour but some are lighter, tending to become
fawn, This form is commonly found down to 10 tm but occasionally specimens
hay¥e been taken from deeper water and there is an unusual record of 3 specimens
from 30 m taken by Mr. BR. C. Sprigy off Carickalinga Head in St. Vincent Gulf,
South Australia,
UNIOPHORA NUDA Perrier
Asterias nuda Perrier, 1875, p. 335.
Uniephore gymnonota Clark, 1925, p. 405.
Material Examined. S.A.M, (80 specimens) KI78-9, K522, K599, K636,
K642, KA52,
Perrier’s type was stated to have come from “Port Lincoln, (detroit de
Torres)". A series of specimens taken off Cape Donnington just outside Pt,
A REVISION OF TIT STARFISH GENUS TINIOPIORA 7
Lincoln Harbour. South Australia conforms exactly with Perrier’s description and
vunfirms Clark's view (1928, p, 417) of the place of origin of the specivs,
The species is distinguishable from the “multispina” group by the very small
number and size of its spines, and many specimens, save for the adambulacrals,
are quite denuded of spines. [t is without exception, covered by a thick skin
which tends to conceal the existing spines but does not obscure the praminent
plates forming the carinal, dorso-lateral and marginal series.
Examination of Clark’s type of U. gymnonota shows no significant ditterences
between it and the specimens from Cape Donnington. Clark purported lo clis-
tinguish (7. nude from U. gymnonota on the ground that the lateer did not have
any pedicellariae corresponding to those observed by Perrier in the ambulacral
groove and which he described in these terms “droit, court, large, en forme de
triangle”, ,... However there are similar pedicellariac in Clark's type and in
many other specimens from the north coast of Kangaroo Island and Spencer Gulf,
South Austialia and it is concluded that Clark’s differentiation was in error.
‘This species has a greater depth range and diversity of habitat than LU’ grani-
fert. The specimens from Cape Donnington were taken in 14 m trom thick
beds of the hammer oyster Malleus meridianus Cotton. Several specimens were
observed feeding on the oyster and this no doubt constituted their principal diet.
In Nepean Bay near Kingscote, South Australia in 5-8 m there ure Marge colonies
inhabiting the beds of the angiosperms Zostera sp, and Halophila ovalis (KR.
Brown) Hooker, There it feeds on bivalves and on small tunicates which find
a ready attachment to debris and rocks scattered on the bottom, It also occurs
in deeper water off the north coast of Kangaroo [sland and in Backstairs Passage,
South Australia, in 20 to 40 m on rocky or shellyrit bottoms, I), colour the spocies
varies from reddish brown to fawn, the specimens from deeper water being
invariably the lighter in colour.
UNIOPHORA DYSCRITA Clark
Univphora dysorita Clark. 1923, p, 244.
A total of 15 specimens have been examined from the private collection of
Dr. E. FP. Hodgkin all of which are referred to this species. There are 5 jnvenile
specimens numbered U.D. 9-15 from deep water (120 to 200 m) and the remain-
er are from shallow water. The specimens show considerable diversity anc one
or (wo approach U, granifera (sinusoida form) in appearance; but in the main
the species is quite distinctive,
In four specimens numbered U.D, 1-4 froin Rockingham and Woodman’s
Point near Fremantle, Western Australia, the spines on the carinal series are
stout at the base and conieally pointed. These spines are often 2-3 mn long
and 0:5-0°7 mm in diameter at their base, and number from 25-30 along the
earinal line. There are also 20 or more much smaller spinelets along the same
line. Elsewhere on the dorsal surface there are many fine spinelets up ty
0-35 mm long on the plates. One of these (U.D, 1) is shown in Plate 1, These
specimens conform to Clark's deseription execpt that the carinal series is mare
evident than appears to be so in the type. In four other specimens numbered
U.D, 5-8 from Woodman’'s Point, Cockburn Sound and Carnac Island, Wester
Australia, the dorsal spines on the carinal series and elsewhere are predominantly
capitate and globose, A few of the spines are rather bluntly pointed, Apparently
there is considerable variation in colour in the species. The colour dorsally
ranges from dark red to fawn and in some specimens the papular areas ave a
ereenish-brown. Below the colour is pranze. Most of the specimens were taken
on rocky hottom but several are reported from muddy or sandy bottom.
5 5. A. SHEPHERD
‘Two specimens uumbered U.D. 14 and 15 present some difficulty by reason
of their extraordinary spinulation, One of these, U.D. 14 is shown in Plate 1.
They were both taken at the Naval Base, Cockburn Sound, Western Australia.
Thwse specimens differ from those described earlier in having few stout spines
but many more fine bluntly pointed spinclets often about 1 mm long and
0-3-0-6 mm in diameter, some of which are slightly flattened at their distal ends
aml somewhat chisel-like. The carinal plates are very sinuous and obscure and
with the dorso-lateral plates enclose large polygonal arcas devoid of spines. The
spines on the carinal plates number from 80-100 on each arm, The marginal
spines and actino-lateral spies are not as flattened or as chisel-like as the
specimens described above. A few of the actino-lateral spines are divided inta
fvo or three short branches but this is nota distinctive feature of the species
us Clark asserts (1928, p. 417). It is not considered that the differences in
these two specimens are of sufficient magnitude to justify separation and in view
of the cliversity shown by the other specimen, they are believed to represent at
most a variant form. They were reported to have been taken at 3m depth on
bite from which it may be inferred that their habitat is a sandy or muddy
suittorn..
The juvenile specimens, the largest of which has R/r = 22/4 mm were all
dredged off Rottnest Island, Lancelin Island or Cape Naturaliste, Western Aus-
tralia, It is noteworthy that in one specimen (U.D. 9) the innermost series of
actinal plates nearest the adambulacral armature carries 3 spines on each plate.
In the other 4 specimens there are only 2 t each such plate. Otherwise there are
no notable differences other than those une would expect Lrom juvenile specimens,
The absence of adult specimens from deep water off Western Australia as
for South Australia lends credence to the view that this is a shallow water species
and that the specimens from deep water are expatriates which having settled
there as larvae, do not find favourable conditions for survival to maturity.
The adnit specimens show considerable variation in the character o! the
spines but there is no doubt that they are conspecific. Having regard tu their
diversity which at one extreme approaches U. granifera “granifera” group there
exists some doubt whether this form should be given specific status. Taken
individually, none of the characters nsed by Clark (1923, p. 244 and p. 246) in
eteating the species ure reliable and each of them iy shown at least in some
degree by one or other of the South Australian forms. On the other hand the
overall appearance of the majority of specimens is unlike that of any seen from
South Australia or elsewhere. The occurrence in some specimens of larger and
relutively long pointed spines on the rays and disk is distitetive and the clusters
of fine and pointed spinclets on the carinal and dorsu-lateral plates in uthers
are umiygne in the genus. On the whole the species is considered valid.
An endemic distribution in the temperate waters of the lower west coast
of Western Austral is indicated from the preserit material, No specitneny have
been cecorded from the Great Australian Bight, From the brief wotes accom-
panying the specimens the species shows some variability in habitat and may
occ on rock, sand, or muddy bottom in depths ta 20 m.
Distribution in the South Australian Gulfs
Uniophora granifera is seldom found on exposed coastlines; it prefers pro-
tected waters and occurs predominantly along the coustal fringe of gulfs and hays
dows to wbont 15m, Occasionally juveniles with R np ta 10mm have heen taken
in deeper water of 40-50 m but this environment is apparently unsuitable as
larger specimens have never been taken al such depth despite extensive collecting
and dredging,
A REVISION OF THE STARFISH CENUS UNIOPHORA 9
Uniophora nuda is found in the protected parts of more open waters but so
far has not been taken in St, Vincent Gulf.
Figure 1 indicates the distribution of the species in the Gulfs,
Populations of “granifera” group occur in abundance on the reefs of the
eastern coastal margin of St. Vincent Gulf southwards from Glenelg. These reefs
are not continuous and colonies of the seastar are geographically separated by
LEGEND
UNIOPHORA GRANIFERA
"granitera’ group *
Common type.
globifera
sinusoida
fungifera
>7~mw
"multispina’ group rs
UNIOPHORA NUDA ao
qx
O/Pt. Hughes
Spencer Gulf
Sir
Sa Joseph Banks
Vincent
Kangaroo = Island
Fig, 1. The distribution of the species in Spencer and St. Vincent Gulfs showing the occurrence
of the dominant forms.
1) S. A, SHEPITERD
stretches of sandy bottom, ‘There are not many representatives of the “sinusoida®
form here; the “fungifera” form is dominant at Glenelg, in Holdfast Bay and
Halletts Cove but further south the “globifera” form is more common. The
population samples are not sufficient to assess accurately the proportions in whieh
the three forms occur. It is noted however that the specimens of the dominant
form from any one locality are fairly homogeneous and that there are minor hut
tecngnizable morphological differences when a population sample from one place
is cumpared with onc from an adjacent colony, The inter-population differences
do not appear to follow any pattert of variation and no clines have heen detected.
The distribution wf populations of “muiltispinw” group corresponds with the
extent of the beds of Posidonia and Cymaducia on the coastal margins of St.
Vineent Gulf, Tt is found along much of the westcrn margin of the Gulf but on
the eastern margin it is common only to the north af Holdfast Bay; specimens
are seldom taken to the south.
Some intergradation between U. nuda and “mullispina” forms of U. granifera
has been observed on the north coast of Kangaroo Island near Cape Marsden and
about Eastern Cove (Clark, 1928, p. 411) but its extent is not known, ‘Ihe
evidence does not suggest that it is at all frequent er widespread. No inter-
gradation has heen observed anywhere between U, nuda wud any forms of
“granifera” group even where the two species are found in the same geographical
arva, although in different ecological niches.
The distribution in Spencer Gulf is still sketchily known. Despite extensive
diving no specimens have been taken around the Gambier Islands, the Neptunes,
or Thistle Island but they seem to be common enough in the quieter waters
further north, In the Sir Joseph Banks Group it appears that Uniophara
granifera occurs commonly both with the “granifera” and “multispina” kind of
spinulation (Stach, 1938, p. 329), and WU. nuda has also been dredyed in deeper
water off Spilsby Island.
No specimens of U. vranifera have been taken west of Spencer Culf bul as
little collecting has been done an the west coast of Eyre Peninsula its discovery
in suitable localities along that coast would not be surprising. As vet only
UU, granifera “granifera” group has heen taken off the coasts of New South Wales,
Victoria and Tasmania,
Differences in Uniophora Colonies
The forms differ basically from each other in the number and nature of the
spines, notably those dorsally on the rays, Spine counts therefore seem to offer
the best method of presenting the differences statistically despite the irregularity
ot arrangement of the spines. The spines along the plates of the carinal series
from the base of the ray to the tip were counted and the results are expressed in
spines per cm lo compensate for size variations.
Because of the unpredictable local occurrence of colonies there ure not
many collections which ure sufficiently comprehensive to give reliable statistical
definitions of the several populations. For the sake of completeness even smull
series are analysed so that the data in the following table and Figure 2 comprise
the figures for all series of Ave or more specimens.
The purpose of the statistical record is firstly tu show the close relationships
between the several forms and sceandly to determine the yariability within a
population and so complete the empirical description of the material, Analysis
of the larger pupulation samples = thal the spine-counts follow a normal
distribution curve and 2 comparison of population samples indicates 2 gradual
A REVISION OF THE STARFISH GENUS UNIOPHORA ll
TABLE 1
Geographical occurrence of Uniophora cclonics sampled.
Mean size
Form Locality + Depth (in metres) No. of | of sample
specimens | (R) in cm.
(1) U. nuda Cape Donnington—lim. 5 8-3
(2) a Sir Joseph Banks Group—30m. 6 4:3
(3) " Kingscote—Nepean Bay—5m. 57 4-5
(4) 5 . ” Backstairs Passage—30m, 5 8-8
5) U. granifera
(“multispina” group) Edithburgh—im. 28 4:5
(6) se Outer Harbour—5m. 10 47
(7) 3 Semaphore—10m. 17 10-2
(8) 33 Pt. Turton—7m. 14 6°8
(9) U. grantfera
(‘‘granifera,”’ group) Glenelg Breakwatcr—5m. 7 7-5
(10) 9% Halletts Cove—7m. 7 6-0
(11) ba Pt. Noarlunga—7m. 34 4-6
(12) + Pt. Willunga—8m. 21 4-0
(13} ” Snapper Rock off Cape Donnington—im. 6 6-4
(14) 3 Pt. Hughes—5m. 6 4-6
U. granifera (multispina gp.d
oO 2 4 6 8 10 12 14 16 16 20 22 a4 26
Spines per cm.
Fig. 2. The graph is a summary of Uniophora carinal spine-counts. In cach case the single
line represents the range, the rectangle in block one Standard Deviation on either side of the
mean, and the vertical line the mean.
1z S. A. SHEPHERD
increase in spine counts from U, nuda to U, granifera. Despite the slight overlap
between U. nuda and U. granifera it is considered that the combination of the
differences between the two is sufficient to justify specific differentiation. Table
2 summarises the characters which are useful in discriminating between the
forms. It is evident at once, that there are no diagnostic characters which can
he relied upon as absolute determinants; the characters are all variable and can
be used only in conjunction with others to distinguish the forms. Even then the
degree of overlap may in some cases cause difficulty. Another problem is that
Table 2 is based primarily on the South Australian material so that when the
specimens from other States are examined it is found that the character com-
binations are not quite the sare and intermediate degrees of relationship exist.
Other characters are referred to in the literature which have been used from
time to time as determinants, for example the presence of pedicellariae and
pebhled areas in the intermarginal plates, but these are now ignored as they
have not been found to be of any significance.
TABLE 2
Major differences between Uniprora species;
|
| UU gpremifera
di, dyserita. CT. render |
| “eranitera’* op. “multispina” op.
Carinal series. Ziy-war Straight, some- | Zig-cag sometimes | Straight, some-
ic. central series times 7ig-2ag irregular times: Zig-zag
of plates dor- distally i distally
anally on rays ! |
Carinal spines | Capitate or [neonspiewous Capitate, singly or | Capitate some-
Frequency | blantly pointed | fine sane In ganips tines blantly
(per em.) 9-15 pointer $-25 pointed singly or
| 0-3 Mm groups:
4-13
Dorso-latoral Jrregularly Absent Trregularly Form Lor 2
spires arranged, often arranged, or repular series each
in groups, | arranged to form | side of carinals
Smaller and pelygenoal papular
finer than | debs
varinals
Supero- Capitate ur | Rare or absent | Capitate Slightly capitate.
marginal spines | fatrened Often in groups
(orminally j of 2-3
Actino-lateral Fresent | Rare br absont | Present Present
spines |
The considerable increase in spine numbers per cm along the carinal line
in “granifera” group as shown in Figure 2 is due partly to the exaggerated
development of the characteristic zigzag carinal plates and partly to the increase
in spines on the plates. Of the series from St. Vincent Gulf it is noteworthy
that the specimens from Port Noarlunga sonthwards are generally stnaller and
have fewer and more capitate spines than those further north. The series from
Halletts Cove and Glenelsy Breakwater shows some intergradation with “multi-
spina” group,
A REVISION OF THE STARFISH GENUS UNIOPHORA 1
Table 1 also shows the variation in the mean size of adult specimens from
the populations sampled, The reason for the diversity in size is not known. It
does not appear to be related directly to age as there is no difference in maximum
size of specimens collected in one locality at different times of the year and in
different years. The seastars are sedentary in habit and it is probable that the
Ope and quantity of food available is an important factor. It is noted for example
that the specimens of U. nuda from the rich hammer oyster beds off Cape Don-
nington are considerably larger than the specimens of the samie species from the
quiet waters of Nepean Bay, Kangaroo Island.
U. dyscrita UU. nudo U. granifera
granifera gp. multispina gp.
Fig. 8, Lateral view of prominent carinal spines on rays.
CONCLUSION
The greater amount of material now available reveals that in the South
Australian Gulfs there are two species of Uniophora, One of these U. eranifera
contains two component groups of populations, each of which has some pecu-
liarities of behaviour, distribution and morphology. The populations called
“granifera” are found on rocky bottom along coasts of moderate wave action
whereas “multispina” populations oceur on sandy bottom and in calmer water,
Specimens having characteristics of both “granifera” and “multispina” have been
taken on bottoms of.a mixed character, The interesting problem is raised whether
the differences in morphology are genetically or ecologically determined, but this
cannot be resolved without experimental work,
The existing evidence suggests that U. uucde is a distinct species but this
view may require reconsideration should intermediate populations be discoyered,
Whatever the case is, the two species have succeeded in occupying a varicty of
habitats and so been able to fourish in the Gulf regions in an abnndance, which
is without rival among the asteroids, There is nu evidence of the species
achieving the samc success elsewhere on the Australian coast.
Uniophora dyscrita must be retained as a valid species for the present.
There is no record of the species from the Great Australian Bight, It is quite
likely that the exposed coasts and long stretches of sandy shore of that region
constitute a nalural barrier sufficient to prevent gene flow between the South
Australian and Western Australian species. (See Womersley and Edinonds,
1958, p. 221, and Jennings, 1963, p. 45.) In view of the known ecological
requirements of the specics much of this coast would not provide favourable
conditions for survival. The differences already visible indicate genctic variation
and hence the evolution af separate species.
i4 5S. A, SHEPHERD
ACKNOWLEDGMENTS
I am grateful to members of the Underwater Research Group who assisted
me in collecting specimens from time to time, to Mr. R. C. Sprigg who generously
made available the research vessel Saori for numerous field excursions, Dr. E. P.
Hodgkin and Mr, I. M. Thomas read the manuscript and offered valued advice.
Finally I am grateful to Miss E. Pope and Miss J. H. McPherson who sent to me
the collections of the Australian Museum and the National Museum of Victoria
respectively, and to Dr, E, P. Hodgkin who sent his personal collection.
REFERENCES
Crark, H. L., 1923. Journ. Linn. Soc. (Lond.) Zool., 35, pp. 244-246.
Crarx, H. L., 1928. Rec. §.A. Museum, Vol. Ill, pp. 403-417.
Crark, H. L., 1946. The Echinoderm Fauna of Australia, pp, 158-161.
Corton, B. C., and Goprrey, F. K., 1942. Rec, S.A, Museum, Vol. VII, p. 193.
Fisuer, W. K,, 1923. Ann. Mag. Nat. Hist. Ser., 9 Vol., 12, p. 597,
Fisner, W. K., 1926. Ann, Mag. Nat. Hist. Ser., 9 Vol., 18, p. 198.
Gray, J. E., 1840. Ann. Mag. Nat. Hist., 6, p. 288.
Jennincs, J. N., 1963. Trans. Roy. Soc. S.Aust., 87, pp, 41-62.
Lamarck, J. B. P., 1816. Anim, s. Vert., ii, p. 560.
Perrier, E., 1875. Arch. Zool. Exp., iv, pp. 335-345.
Sracu, L. W., 1938. Proc. Roy. Soc. Victoria, 50 (N.S.), pp. 329-332,
Womers.ey, H, B, S., and Epmonps, S. J., 1958. Aust. J. Mar. Freshw. Res., 9, pp. 217-260.
S, A. SHEPHERD
(2) Dorsal view of specimen of Uni-
ophora dyscrita numbered U.D,
14 R = 55 mm.
Collected Stn. 61 Naval Base, Cockburn
Sound, W.A., among Pinna 10 ft.
deep by Marine Gp W.A. Naturalists
10/4/60. (Photo E, P. Hodgkin. )
PLATE 1
Pirate |
(1) Dorsal view of specimen of Uni-
ophora dyscrita numbered U.D. 1
R = 54 mm. Collected R. Howlett
on muddy. sandy bottom, Depth
25 ft. Palm Beach Jetty 3/3/60.
Rockingham, W.A. (Photo E. P.
Hodgkin. )
PRELIMINARY PALAEOMAGNETIC RESULTS FROM THE ADELAIDE
SYSTEM AND CAMBRIAN OF SOUTH AUSTRALIA
BY J. C. BRIDEN*
Summary
The natural remanent magnetization (NRM) of some sediments from the Adelaide System and
Cambrian of South Australia is reported. In some of the formations, which were studied, notably the
Cambrian sequence on Kangaroo Island and the Billy Creek Formation in the Flinders Ranges,
directions were consistent with an NRM of Mesozoic or early Tertiary age. It is suggested the NRM
in the Cambrian of Kangaroo Island was acquired during a period of slightly elevated rock
temperatures and stabilised by cooling to near present day temperatures. In the Marinoan and
Cambrian sediments of the Flinders Ranges, the secondary NRM may be due to a surface effect,
which resulted in increased grain size of the magnetic fraction.
PRELIMINARY PALAEOMAGNETIC RESULTS FROM THE ADELAIDE
SYSTEM AND CAMBRIAN OF SOUTH AUSTRALIA
by J. C. Bruwen®
(Communicated by B. Daily)
[Read 12 September 1967]
SUMMARY
The natural remanent magnetization {NAM) of some sediments from the
Adeluide System and Cambrian of South Australia is reported. In some of the
formations which were studied. notably the Cambrian sequence on Kangaroo
Island and the Billy Creek Formation in the Flinders Ranges, directions were
consistent with an NRM of Mesozoic or early Tertiary age. It is suggosted the
NRM in the Cambrian of Kangaroo Island «yas acquired during a peried of
slightly elevated rock temperatures and stabilised by cooling to neur present day
temperatures, In the Marinoan and Cambrian sediments of the Mlinders Ranges,
the secondary NRM may be due to a surface effect. which restted in increased
train sizo of the magnetic fraction.
INTRODUCTION
The natural remanent magnetization (NRM) of some sediments from the
Adelaide System and Cambrian of South Australia is reported. In some of the
formalions which were sludied, notably the Cambrian sequence on Kangaroo
Island, and the Billy Creck Formation in the Flinders Ranges, directions were
consistent with an NRM of Mesozoic or early Tertiary age. It is suggested that
the NRM in the Cambrian of Kangaroo Island was acquired during a period
of slightly elevated rock temperatures, possibly connected with early Tertiary
igneous activity, and was stabilised by cooling to near present-day temperatures,
In the Marinoan and Cambrian sediments of the Flinders Ranges, the secoudary
NRM may he duc to a surface effect which resulted in increased grainsize of the
magnetic fraction. Results from other formations, in which NRM is weak in
intensity and scattercd in direction, are reported in brief, because consistency of
direction was evident in isolated portions of the sequences; although their
significance cannot he assessed with such limited data, they may be important
in the light of further work which is in progress in the State,
SURFACE COLLECTIONS
The procedure in the field was to collect from | to 6 samples from each
site, Up to 4 specimens were cut from each sample, in which direction and
intensity of NRM were measured in the laboratory using an astatie magnetometer,
Direction is quoted in terms of declination (D) and inclination (1, regarded as
positive downward from the horizontal) relative tu two sets of axes: (1) relative
Trans. Roy. Soc. S. Aust, (1967), Vol, 91.
18 J. C. BRIDEN
the folding of the beds on the assumption that each phase of Folding has been
purely rotational (“corrected”), Directions are analysed by the method of Fisher
(1953). Stability of NRM is assessed (1) by comparison of the uncorrected
roean direction with the present field, (2) by comparing the estimate of pre-
cision (k) of grouping of directions before and after correction for folding (if
corrected directions are more precise, then NRM may be presumed to be older
than the folding), and (3) by interpreting the thermal demagnetization charac-
teristics of specimens in the laboratory.
VABLE 1
Sammary of palacomagnetic measurements in the Adelaide Syste.
Series Formation Locality of | Comments
Samples |
Pound Quartzito Railway cuttings 14 | Weak and widely
equivalent through South scattered NAM with
ABC Range Hummocks Ranges 3 negative inclinationa
Quartzite equivalent relative tu the
Upper Glacial 5 present horizontal
Sequence’
MARINOAN ——_—- - —
Sandatones and Hallett Cove 35 3 sites near middle of
arkoses (14 sites) aAquence consistent.
Correeled mean after
cleaning at 400°C
D191, i = +34",
k-5
Sandstones Reynetla Quarries 10 4 sites consistent,
(5 sites) initial corrected mean
B=? T= 411",
| hk = 35
Brighton Limestone | Heynella Quarries 3 Weak and widely
Happy Valley z scattered NRM with
ve THN Satie , -H: & neyative (upward)
stumiran | Papley Hill Glstos, | Tepler Hilt j | inclinations rlative
to the prosont
Sturt Tillite Loeckler Road Quarry 1 horizontal
TORRENSIAN | Stonyfcll Quartzite Greenhill Quarries 2 Nob detectablo NRM
Adelaide System:
Results. are summarised in Table 1,
portions. of the sections were NRMs consistent.
Only in isolated
In a small face at the east end
of Reynella Quarries, 4 sites in about 5 m of the lowest Marinoun sandstones
have a mean. direction D = 7°, T = 11° after correction with k = 32. A fifth
site, only a few metres away in another face, was not in agreement, The coastal
section north and south of Hallett Cove was sampled thoroughly, but only at
three sites near the northern end of the cove were directions consistent. The
increase in precision after thermal cleaning at 400°C and correction for folding
(D = 191°, f= +39°, k= 5) compared with the uncorrected mean direction of
total NRM (k = 1) suggests that a relic of stable NRM which is older than the
folding may have been preserved,
PALAEOMAGNETIC RESULTS. ADELAIDE SYSTEM AND CAMBRIAN OF S.A. 19
Cambrian: Twenty-three sites were sampled in the Cambrian sequence on
the north coast of Kangaroo Island (Duily, 1957). The distinction between the
Emu Bay Shale and the equivalent of the White Point Conglomerate near Emu
Ray depends on the recognition of a Redlichia horizon which also occurs in the
Vlinders Ranges, not far below the base of the Billy Creek Formation. Because
the author did not find the Redlichia horizon, 3 sites included with the White
Point Conglomerate might strictly belong to. the overlying formation, In_ this
context, the distinction is not important because the palacomagnetism vf the
Kangaroo Island Group does not vary from formation to formation. All site
mean directions except one (near Point Marsden) were significant with 95 per
cent probability. Before correction for folding all inclinations were steep, and
at all except three sites were directed upwards (in the same sense as the present
field, and referred to as “normal’). At 2 sites, however, in the Emu Bay Shale
in its eastern section, steep downward inclinations were observed (called
“reversed"), and at a third site, nearby, both normal and reversed samples were
found. The mean direction after adjustment for the reversed directions, is
slightly steeper than the present field (Figure 1) and is more preciscly defined
than when correction is made for folding (Table 2).
TABLE 2
Analysis of NRM directions in Cambrian stdiments fon Kangaroo Taland.
| |
t pale
8B gn | 7 & a
uncorrected 23 3AT7 75 UT-5 6 agW Gan
carrectent 22 289 =73 7-9 IL —_—_ —
Bis the wumber Hf significant sites (05 per cent prohahility): |
is the semi-angle of the 95 per cent cone of confidence; (4, A) ia the palacumugnatie pole,
Initial directions of NRM in the Billy Creek Formation are steeply upwards
(Figure 2.) Upon thermal demagnetization, direction changes at most sites (at
the north of Lake Torrens, in the Copley-Mount Scott district and between
Wirealpa and Martin Well) are irregular, but tend in general towards a
southwesterly direction, At Balcoracana Creck (Figure 3) directions change
systematically until, after heating to 500°C and correcting for folding, the mean
is horizontal and southwesterly, which is in agreement with that found in other
Cambrian rocks in Australia by Irving and Green (1958). This suggests that,
although the dominant component of NRM is secondary, in at Teast part of the
formation a relic of more stable NRM is preserved, and it is possible that this
is of Cambrian age.
BORECORE SAMPLES
Measurements of NRM of borecore samples are limited hy lack of azimuthal
orientation: inclination but not declination can be measured. Nevertheless such
measurements are useful for estimating inclination in areas where rocks at the
surface have been remagnetized, since it is possible that primary magnetization
might have been preserved at depth. Briden and Ward (1966) devised a
method of estimating mean inclination and Fisherian precision from a collection
of borecores, which has heen nsed in aualvsing results from South Australia and
the Northern ‘Territory (Table 3), A vertical mark was made on each sample,
and twa discs were cut from each, so that consistency of NRM direction within
a sample could be tested; when differences cxcecded 30°, results were discarded.
20 J. C. BRIDEN
TABLE 3
Analysis of inclination of NRM in borecores,
B is the number of consistent samples; A, is the palacolatitude.
—e—,;,CaKX—————— eee
Borehole and location Age B I k: Ay
Upper
BMR/GRG No. 7 (136-1°E, 22-3°S) Cambrian 8 —15] 85 9
Upper
BMR/GRG No. 5 (135-2°E, 21-+3°8) Cambrian 8 —42] 21 24
Lower
Minlaton No, 1 (137-7°E, 34-8°S) Cambrian 13 —55 5 35
1340-1750 ft. | Upper 21 | —85| 25 | 80
Wilkatana No. 1 (138-0°E, 32-2°S) 1740-1845 ft, Marinoan 5 —4] 20 24
Lower 23 —36 6 20
Clarence River No, 1 (136-5°E, 31-1°S8) Marinoan
eee CO ee
Fig. 1. Site mean directions
and thermal demagnetization of
NRM in Cambrian sediments
from Kangaroo Island. (a)
Stereographic projections of
uncorrected (left) and correc-
ted {right) directions. At one
site where polarity is mixed,
the means of both normal and
reversely magnetized samples
are shown, and are joined by
the broken line. The mean
NRM direction is denoted by a
star, with the circle of 95 per
cent confidence around it, The
directions of the present and
axial dipole fields are denoted
by P and D, (b) Thermal de-
magnetization curves of samples
KI5, KI19, KI57;_ intensities
(m) are normalized by divid-
ing by the total NRM intensity
(M,). Open symbols denote
upward and solid symbols
downward inclinations.
PALAEOMAGNETIC RESULTS, ADELAIDE SYSTEM AND CAMBRIAN OF 5.A. 21
In the Wilkatana No. 1 bore, there is an abrupt change in inclination at
about 1,750 ft, so the groups above and below that level have been analysed
separately. In Clarence River No. 1, inclinations are in two groups (Figure 4)
with moderate positive and negative inclinations respectively. This suggests not
merely a large scatter of directions, but rather that some of the cores have been
marked the wrong way up. (An alternative explanation in terms of reversals
of NRM is not considered plausible because there is no discernible stratigraphic
pattern in the distribution of the two groups.) From the mean inclinations, the
palacolatitude (A,) of each borehole is calculated on the assumption of a
geocentric dipole field from the relation
tani, = 2tana,
and the results are compared on a map of palacomagnetic poles (Figure 5) with
results from other Australian rocks,
1.2-
1.0
M 57
M
° 08
19
0.6
0.4
5
0.2
100 200 300 400 500
Temp, °C
DISCUSSION OF THE ORIGIN OF SECONDARY NRMs
Thermal demagnetization curves of the Billy Creek Formation and Emu
Bay Shale (Figures 1 and 3) are similar to those of ancient secondary magnetiza-
tions in the Bloomsburg red beds ({rving and Opdyke, 1965) and the Old Red
Sandstone (Chamalaun, 1964). The hypothesis which is proposed for their
origin is that they were acquired in the Earth’s field over a long period (say 10%
years) after which the effective relaxation times of the magnetic grains were
increased. This has the effect of “freczing-in” the NRM so that it may be stable
over millions of years at normal temperatures, Increase in relaxation time may
bo
hw
J. C. BRIDEN
uncorrected
Fig. 2. Thermal cleaning of Billy Creek Formation, Initial directions. and directions after
heating to 200°C and 400°C, both before and after correction for folding, Sites are NEW
(northeast of Wirrealpa); YC (Yarra Wurta Creek); LT (edge of Lake Torrens); Cl and C3
(Copley-Mount Scott); Bl and B2 (Balcoracana Creek); TMC (Ten Mile Creek) and E
(Eregunda Creek). Open symbols denote upward and solid symbols downward inclinations.
PALAEOMAGNETIC RESULTS, ADELAIDE SYSTEM AND CAMBRIAN OF S.A, 23
N
Vig. 3, Thermal demagnetiza-
tion of two specimens from
Balcoracana Creek, in steps,
at room temperature, 100°C,
200°C, 300°C, 400°C, 450°C,
and 500°C. The stereogram
(above) shows the change of
uncorrected directions (circles)
with progressive demagnetiza-
tion. in the sequence indicated
by the arrows, and (squares)
after demagnetization to 500°C
and correction for the tilt of
the beds, which is also shown.
The demagnetization curves
(below) show vectorial mean
intensity of the two specimens.
Open symbols denote upward
M x10°%e.m.u./gm and solid symbols downward
2 inclinations.
Tere) 300 500 °C
be due to fall in temperature, (due to uplift during folding, or at the close of a
phase of igneous activity), change in grainsize, or chemical change. For the
Bloomsburg Formation and the Old Red Sandstone, fall in temperature has
been proposed.
On Kangaroo Island, Lower Tertiary basalts outcrop on the low hills inland
from the palaeomagnetic sampling sites. It is not unreasonable to suppose that
they were formerly more extensive, and that temperatures in the Cambrian rocks
were elevated at the time of their extrusion. The mean direction of NRM in
these rocks is similar to that found in early Tertiary rocks in Australia (Irving,
1964) and hence the NIM may be the same age as the basalts. The most
reasonable interpretation is that only the reversed rocks retain their NRM from
that time, and that the normal rocks have NRM of recent origin.
a4 J. C. BRIDEN
UP
ae 4 iyplieitions My, NRM in
arence River No. 1 (Woomera
HORIZONTAI: bore,
The inclinations in borecore samples are, for the most part, not inconsistent
with NRM of comparable age to their host rocks. But in the Wilkatana No. |
bore, the upper part of the sequence appears to have been remagnetized in a
direction steeper than the present field. This may be due to a surface effect
operative in the Mesozoic or early Tertiary (Figure 5), and it is possible that this
was a regional cffect which involved the Billy Creek Formation also. There is
no geological evidence of elevated temperatures in these rocks, and it may be
that chemical or grainsize changes were responsible for stabilising the NRM.
The acquisition of viscous magnetization (which increases with the time
of application of a magnetic field) at various temperatures by specimens of Billy
Creck Formation and Emu Bay Shale has been investigated in the laboratory
and is described by Briden (1965).
ACKNOWLEDGMENTS
The work was carried out at the Australian National University, under the
guidance of Dr. E. Irving, to whom I am indebted for much advice. The
Director of the Geological Survey of South Australia allawed me access to
unpublished maps and information, and to the collection of cores. I wish to
thank officers and former officers of the survey (especially Messrs, B. P, Thomson,
B. P. Webb and A. R, Crawford) for their co-operation and for guidance in the
field, and Mr. R. Dalgarno, who collected the samples from Balcoracana Creek.
PALAEOMAGNETIC RESULTS, ADELAIDE SYSTEM AND CAMBRIAN OF S.A, 25
Dr. B. Daily gave me the benefit of his detailed knowledge of the Kangaroo
Island Group. The Director, Bureau of Mineral Resources, Geology and
Geophysics, Canberra, allowed me access to the cores from the Georgina basin,
Fig. 5. Loci of palaeomagnetic poles. calculated from borecore measurements, by
drawing cireles of radius },, centred on. the drilling sites. 1; Clarence River.
2; Wilkatana (a = upper. b = lower). 3: Minlaton. 4: GRC5. 5: GRG7.
The curve is the approximate polar wandcring curve for Australia. constructed
from the A-¢roup data of Irving (1964); dashes for late Precambrian to Devonian,
dots tor the Carboniferous, solid line for the Mesozoic and dot-dash for the
Cainozoic.
REFERENCES
Brinew, J. G., 1965. Ancient secondary magnetizations in rocks. J, Geophys, Res.. 70, pp.
5205-5221,
Brien, J. C.. and Warp. M, A., 1966, Analysis of magnetic inclination in borecores. Pure
and Appl. Geophys., 63, pp. 133-152.
CHAMALAUN, F. IT,. 1964. Origin of the secondary magnetization in the Old Red Sandstoncs
of the Anglo-Welsh cnvette. J, Geophys. Res.. 69, pp. 4327-4338.
Daiwy, B., 1957, The Cambrian in South Australia, Bureau of Mineral Resources, Bulletin
No. 49, pp. 91-147, Carberra.
Fister, KR, A.. 1953. Dispersion of a Sphere. Proc. Roy. Soe. London, A, 217, pp. 295-305,
Invinc, E., 1964. Paleomagnetism, Wiley, New York.
TRvING, ie and Grrex, R., 1958, Polar movement relative to Australia. Geophys. J., 1,
pp. 64-72,
Invinc, E., and Orpyxe. N. D., 1963. The palcomagnetisrn of the Bloomsburg red heds and
its possible application to the leclonic history of the Appalachians. Geophys, J., 9.
pp. 153-167.
ON THE RADIOACTIVITY AND RELATED FLUORESCENT PROPERTIES
OF SEDIMENTARY AUSTRALIAN ZIRCONS
BY I, A. MUMME*
Summary
The natural radioactivity of sedimentary zircons from various placer deposits in Australia was
investigated with a gamma-ray spectrometer.
The radioactivity of the zircon samples was generally weak, and was shown to be due to uranium
series; however, in one sample traces of thorium series were also detected.
Under ultraviolet light many of the colourless to lemon brownish zircons fluoresced with a brilliant
yellow colour which was attributed to the presence of uranium in solid solution.
ON THE RADIOACTIVITY AND RELATED FLUORESCENT
PROPERTIES OF SEDIMENTARY AUSTRALIAN ZIRCONS
by I. A. Musme*
[Read 11 May 1967]
INTRODUCTION
The natural radioactivity of sedimentary zircons from yarious placer deposits
in Australia was investigated with a gamma-ray spectrometer,
The radioactivity of the zircon samples was generally weak, and was
shown to be duc to uranium series; however, in one sample traces of thorium
series were also detected.
Under ultraviolet light many of the colourless to lemon brownish zircons
fluoresced. with a brilliant yellow colonr which was attributed to the presence
of uranium in solid solution.
OCCURRENCE AND NATURE OF RADIOACTIVITY OF ZIRCONS
Zircon is widely distributed in Australia as an accessory constituent of
igneous and metamorphic rocks being especially common in the granitic rocks
and only oecurring sparingly in the basic rocks. It is one of the earliest minerals
to crystallize out of a magma.
It is apparently more abundant in plutonic than voleanic rocks.
By disintegration of these rock types it is concentrated by the action of
water in sedimentary deposits along with other characteristic minerals including
magnetite, garnet, ilmenite, corundum.
As the mineral zircon (ZrSiO,) may contain uranium and thorium as sub-
stitution solid solutions up to 0-1 per cent and even higher amounts as crystal
inclusions, the radioactivity of sedimentary zircons from various placer deposits
in Australia was measured with a gamma-ray spectrometer, and the uranium
and thorium contents estimated by calibration with standard samples.
THE GAMMA-RAY SPECTROMETER
The gamma-ray spectrometer offered a rapid and accurate method of
analysis of the uranium and thorium contents of the zircon concentrates.
The spectrometer employed an electronic means of differentiating between
the energies of the various intercepted gamma-rays.
Essentially the gamma-ray spectrometer consisted of a scintillation detector
which converted an intercepted gamma-ray to an electrical impulse, the voltage
of which was proportional to the energy of the absorbed gamma-ray.
* Australian Atomic Energy Commission. Lucas Heights, Sydney, N.S.W.
Trans. Roy. Sow, $. Aust. (1967), Vol. 91.
28 L A. MUMME
This impulse was amplified and passed through an electronic gating circuit
which allowed only pulses of a specific yoltage to actuate a scaler,
Gamma-rays emitted by radioactive nuclides are of characteristic energies
and the intensity of the gamma-radiation emitted by a specific nuclide is pro-
portional to the quantity of the nuclide present in the sample.
The gamma-ray spectrum graphs were obtained by sweeping the spectrum
with a pulse height analyser,
The individual samples of zircon concentrates were weighed and packed in
perspex cups and counted close to the face of a thallium activated sodium iodide
scintillation crystal which was shielded by a lead castle.
RESULTS OF THE RADIOMETRIC INVESTIGATIONS
An examination of the gamma-ray spectra for the various zircon samples
investigated showed that the uranium series were in equilibrium in each case,
This is to be expected as the zircons resist alteration to a marked degree,
and also the age of the zircons are greater than 3-5 x 10° years—the time required
for radioactive equilibrium to be set up by the contained uranium.
The results of the radiometric measurements are presented in Table 1,
TABLE |
Uranium content Thorium content
Locality | (% U,O>%) (% ThOs)
1, Rocky River, Uralla (15662) NSW. 0-101 0-01
2. Anakie, Queensland (D21364) 0-087 < 0-001
3. Strangway's Range, Central Australia (D401) {)-0021 <0-00L
4. Hanging Rock Head of Dunean’s Creek, 4 miles
along Niangula Read (040400) NSW. 0-0108 <0 001
5. Inverell (D16261) N.8.W. 0-0124 <i 001
6. 100 miles N.W. of Augathella (140162) 0-0071 <0-001
7. Bald Nob Creek, Glen Mes (1916314) 4) OOF <0-001
8, Oban (12 miles $8.) (D2776d) N.S.W. 0241 <i) QOL
9%. Sapphire. Inverell (D26298) N.S; W. 0-0153 AOL
10, Back Creek, 27 miles fram Armidale (D19355}
N.8.W- 0-087 <i QO1
11. Oban (D16257) N.S.W. 0-087 <0- 001
Tingha (D37997) N.S.W. 0-047 <0- 001
13. Trunkey (D10108) N.8.W. 0-043 <.0-001
RESULTS OF THE ULTRAVIOLET LAMP TESTS
As zircons arc frequently fluorescent, the samples were tested for this
property with an ultraviolet lamp. The sedimentary zircon samples show a wide
variation of luminosity trom fluorescence under ultraviolet light ranging from
very weak fluorescence to brilliant yellow hues. The activator for the yellow
fluorescence is attributed to the presence of uranium,
The details of these tests ure brought together in Table 2.
RADIOACTIVITY OF AUSTRALIAN ZIRCONS Bt)
TABLE 2
1. Rocky River, Uralla (D15662). Grystals water worn reddish colour, 0+3 cm average
diameter. fluorescence dull yellow.
2%. Anakie, Queensland (D21964). Grystaly water worn pale reddish colour: 0:6 om
average diameter, one crystal vivid red; Huoresconve yellow, few crystals bright yellow,
3. Strangway’s Range. Central Australia (D40160). Crystal fragments angular up to 3 an
diameter, Grey lemon to pale reddish colour; fluorescence generally dull yellow with
patches of bright yellow,
4. Hanging Rock (D40400). Water worn crystals up to 1 em diameter. Brown-lemon
colour; fluorescence bright yellow,
5. Inverell (D16261). Water worn crystals, pale Jemon. few deep red; 0-3 cm average
diameter, few 1:5 em diameter, Huorescence bright yellaw hue.
6 Augathella Hegion (100 miles NW of Augathella) (D40162). Water worn crystals.
colourless, brownish-yellow, associated with black sapphires; Auorescence bright yellow
and spotty yellow.
7. Bald Nob, Glen Innes (D16314). Heddish zircons few colourless, average diameter 0:4
cm, associated with black sapphires; fluorescence dull to bright-yellow Jues,
& Oban (D27764) (12 miles SE of Oban). Water worn orystals. deep red colour, trans-
lucent, up to 2 em diameter. fluorescence few bright yellow,
%. Sapphire. Tnverell district (D26298). Colourless, reddish and deep red, up to L em,
Hunrescence bright yellow.
10. Back Creek (27 miles from Armidale) (D19355). Colourless, Jemon and pale reddish
zircons up to O-5 em diameter; associated with blue and black sapphires; fluorescence
bright yellow.
1L. Oban (D16257), Deep red crystals water worn 0-3 cm diameter (ow average); not
fluorescent.
if. Tingha (1D37997), Crystals water worn: colourless. yellowish, reddish and deep red;
some crystals tetragonal square prisms, roost crystals water worn, Diameter up to 1:5
em; fluorescence bright yellow.
19. Tnmkey (D10108). Crystals water worm. Translucent red, one crystal bright red,
average diameter 0-5 cm, one crystal fluorescent bright yellow, rest of crystals non-
fluorescent,
CONCLUSIONS
Camima-ray spectrometry measurements on zircon samples from a number of
sedimentary deposits in Australia showed that they were all weakly radioactive.
The radioactivity was shown to be due to the presence of contained uranium
series in solid solution. The zircon concentrates from Uralla (Rocky River)
were considerably more radivactive than the other samples and were also shown
to contain detectable amounts of the thorium series.
In samples containing both colourless to yellow-brown zircons and red
zircons, the latter were considerably more radioactive than the former group.
The red colour apparently has resulted from alpha radiation damage from
the contained uranium series held in solid solution, for on beating the red
zircons, the red colour disappeared very rapidly.
Under the ultraviolet lamp it was observed that the colourless lo yellowish
brown zircons fluoresced brightly with a brilliant yellow colour, whereas the
red zircons were non-fluorescent or only weakly so. The deeolourized zircons,
however, did not regain their fluorescent properties.
ACKNOWLEDGMENT
The author is indebted to Mr. O, Chalmers of the Australian Museum,
Sydney, for the loan of the zircon samples.
CRUSTAL THICKNESS MEASUREMENTS IN THE SOUTH EAST OF
SOUTH AUSTRALIA BASED ON THE REGIONAL GRAVITY VALUES
BY I, A. MUMME
Summary
In the course of this project, regional gravity stations were established along the main highway from
Adelaide to Bordertown. In most cases, these stations were close to gravimeter stations previously
occupied by the South Australian Department of Mines, and the Commonwealth Bureau of Mineral
Resources.
The gravimeter measurements were conducted with a Carter Y2 gravimeter, and the gravity values
determined on this traverse are based on an absolute gravity value of 979-7237 gals at the gravity
base station in the New Observatory, which is located in the grounds of the University of Adelaide
(Mumme, 1960; Dooley and Williams, 1960).
The results of this survey were applied to various equations and graphical methods relating crustal
thickness, and Bouguer anomaly, or elevation. Based on this data, an average crustal thickness of 33
kilometres was determined for this general region investigated.
CRUSTAL THICKNESS MEASUREMENTS IN THE SOUTH EAST OF
SOUTH AUSTRALIA BASED ON THE REGIONAL GRAVITY VALUES
by I. A. Muara
[Read 11 May 1967]
In the course of this project, regional gravity stations were established along
the main highway from Adelaide to Bordertown. In most cases, these stations
were close to gravimeter stations previously occupied by the South Australian
Department of Mines, and the Commonwealth Bureau of Mineral Resources.
The gravimeter measurements were conducted with a Carter Y2 gravimeter,
and the gravity values determined on this traverse are based on an absolute
gravity value of 979:7237 gals at the gravity base station in the New Obser-
vatory, which is located in the grounds of the University of Adelaide (Mumme,
1960; Dooley and Williams, 1960).
The results of this survey were applied to various equations and graphical
methods relating crustal thickness, and Bouguer anomaly, or elevation, Based
on this data, an average crustal thickness of 33 kilometres was determined for
this general region investigated,
PREVIOUS GEOPHYSICAL WORK
Regional gravity work had previously been conducted in this yeneral area
by the Geophysical Section of the South Australian Department of Mines
(O'Driscoll, 1961), and also a gravity traverse had been run by the Bureaw of
Mineral Resources between Adelaide and Melbourne (Marshall and Narain,
1954). Before commencing the survey, the writer calibrated the gravimeter by
measuring the gravity interval between the New Observatory and the Mount
Lofty gravity station which was established by Muckenfuss on behalf of the
Wood's hole Oceanographic Institute while carrying out world wide gravimeter
observations with a geodetic Worden gravimeter,
METIIODS USED
The Carter Y2 gravimeter was calibrated by measuring the dial interval
(allowing for instrumental drift) between the New Observatory and the Mount
Lofty gravity station, assuming a gravity interval of 0-1326 gals, and hence a
factor of 0-0809 milligals per division for the sensitivity factor. Gravity dif-
ferences between the New Observatory gravity station and the gravity stations
occupied were obtained by establishing a number of intermediate gravity
stations, measuring the gravity intervals between successive stations, and thus
obtaining the total gravity interval between the New Observatory gravity station
and the particular gravity station measured, Repeat readings were taken in
een verins the gravity intervals, and curves drawn up to allow for instrumental
itt.
Trans, Roy, Soc. S$. Aust. (1967), Vol. OP.
5a 1. A, MUMME
The gravity stations were generally occupied close lo railway stations or
railway crossings for which accurate reduced level data was availuble from the
Records section of the Department of Raibways, Levels were transferred from
the Kailway survey data to the site of the gravity stations with an Abney clino-
meter and staff. The Railway datum levels were based on a datum level 100 ft
below Low Water Ordinary Spring Tide, and a correction of 105-7 ft were
subtracted to correct the levels to mean sea level.
REDUCTION OF RESULTS
The observed gravity values for the gravity stations were reduced to mean
sea level by applying the following corrections; namely, am elevation correction
and a topographic correction.
(1) Elevation Correction
There are two components in the elevation correction, namely the free-air
correction and the Bouguer correction,
(a) The Free Air Correction: This correction docs not consider the gravity
effect of topography but only the increased distance from the centre of the
earth of the gravity station. Duc to this effect, gravily decreases by 000009406
(1 + 00071 Cos* 9) milligals per foot above the surface of the carth providing
there is nothing but air between the carth’s surface and the point where: gravity
is measured (Heiland, 1964). Thus, the elevation correction merely compensates
the gravity readings without altering their sites,
(b) Bouguer Correction: This correction allows for the attraction of the
inaterial hetween the reference station, viz mean sea-level, and that of the actual
uravily station. The term “Bouguer correction” is uscd here in a restricted sense
to designate the correction for the attraction as approximated by considering the
material as an infinite horizontal slab. The attraction due to gravity for.a point
on the surface of such a slab is 0+01276s ht milligals, where o is the density of
the rock between the reference level (which is mean. sea-level) and the gravity
station under consideration, and h is the elevation of the gravity station.
(2) Yopographic Correction
A gravity sraticule devised by Sigmund Hammer (1939) was used to correct
fow the actual topographic features associated with each gravity slation occupied
along this traverse. The 1930 International Gravity Formula was used to obtain
the theoretical gravity valuc Go for each gravily station at mean sea-level.
where Go = 978-049 (1 | 00052884 Sin? 9 — 0-°0000059 Sin? ¢) gals.
Bouguer anomalies for the gravity stations were calculated hy subtracting
theoretical gravity values, for the gravity stations, from the reduced gravily
values obtained by upplying elevation and topographic corrections. As the
vravity measurements were conducted on x revional scale, an elevation correction
af 0-060 milligals per vertical foot was used (which corresponds to a density
of 2°67 grammes per ec) for the following reasons; (a) for this type of investi-
gation geological efleets appear as random disturbances, (b) there is no need
for a high degree of refinement in the method of data reduction in so far as
the elimination of these effects is converned, (c) a value of 2:67 grammes per ec
would appear to be a reasonable value over the entire length of the traverse
for the density of the rock material occurring above mean sea-level, ‘The results
are given in Tables 1 and 2.
CRUSTAL THICKNESS MEASUREMENTS, SOUTH EAST OF S.A. 33
GEOLOGY OF THE AREA
Between Murray Bridge and Bordertown, the gravimeter traverse passes over
a veneer of Quaternary and recent deposits generally masking any evidence of
subsurface structure. The structural pattern of this area is complicated and
bore hole data suggest that the area north of the traverse forms part of the
Murray Basin Proper, while the area south of a line between Kingston and
Naracoorte belongs to the Gambier Sunklands with a zone of structural highs
between the two areas known as the Padthaway Horst comprising metamorphic
rocks, A broad belt of Palaeozoic granitic rocks outcropping along the north-
west to southeast ridge of the Padthaway Horst from Murray Bridge to
Bordertown includes granites of 8 types.
TABLE 1
| \ ] !
Latitude Longitude Location | Hlevation ft. Observed gravity
34° 45-2” 138° 36-3' New Observatory 108 979-7237 pals
85° 0-6! 138° 42-4' Mount Lofty station 1613 979-6448
34" 58-5" 188° 42-7° Mount Lofty Tower 2934 979-5911
Ja” 0" 138° 44-0° Aldgate 1386" 5 979-6627
3h 2-2! 138° 54-4’ Nairne 1238-6 i 979-6681
38° 7T>iY 138° 1-2’ Murray Bridge 46°65 79-7376
35° 15-5" 1g9° 27-1’ Tailem Bend 57 979° TA25
35° 17-7" 139° 49-1' Moorlands 2-4 79-7795
35° BB+! 138° 40-4’ Coomandook 33-3 B79°7977
$a° 34-7" 139° 44-6" Kiki 85°38 179-8034
33° 42-4" 139° 50-2" Coonalpyn 66-4) \ 979-8058
35° 49-3" 139° 55: 5° Culburra 57-3 979-813)
Bae 54-4! 140° 0-5’ Tintinara fad -0 N79 8152
35° 57+" 140° 10-5! Coonibo §7°3 979-8205
36° G+2’ 140° 20-2° Keith { 94-3 979-8566
86° 12-6" Taq? 40+ 1" Wirresy | 202-3 979-8183
36° 18 +8! 140? 452° Bordertown 261-7 979-8347
TABLE 2
Elevation Topographic Reduced Theoretical Bouguer
Correction Correction Gravity Gravily Anomaly
(milligals) (millizals) (gals) (gals) (gals)
6-45 0-19 979-7304 979-7394 —0- 0090
96-78 1:30 79-7429 979-7469 —f)- 0040
200+40 eld 979-7342 979-7441 —0- 0099
82-21 78 979-7467 O79- 7472 —() 0008
74°32 O85 Y70- 7434 970-7498 —U- 0064
2°79 OT 979-7405 979-7562 = 0187
3-34 0-05 974-7659 979-7682 —0- 0023
1:94 O04 979-7815 979-7713 0-1102
2-00 O01 979+7997 9797871 0-0126
p:12 0-01 979-8088 979-7955 00130
a7 D6 0-01 979-8098 979-8065 " 000383
3-44 O02 979° 8165 979-8 1ti4 rQo01
3-24 0-02 970-8184 979-S$223 —0 00389
h- 2d 02 OTU-S847 YTY-4381 —()- 0034
4:66 ()- 2 9$79- 8623 Y79-8388 0-0235
1214 1-2 979- $304 979-8485 —G 0184
15°70 {)+02 979- R504 979+ ROST —0- 0083
34 I, A, MUMME
INTERPRETATION OF RESULTS
The regional Bouguer anomaly shows a gravity low at Murray Bridge which
is possibly due to the presence of the Murray Bridge granite, which has a rela-
tively lower density than the intruded country rock, or due to structural effects
(Mumme, 1963). A large regional gravity anomaly occurs between Murray
Bridge and Coombe with a maximuin value occurring at Kiki. This is probably
due to basement structures associated with igneous intrusions. Another impor-
tant feature of the plan is a sharp gravity anomaly centred on the township of
Keith. It is of interest to note that the gravity highs along this traverse roughly
correspond to magnetic highs (O’Driscoll, 1960) f Fig, 7), and suggest that they
are due to basement highs in the Archaean metasediments whereas the gravity
lows are due to granitic intrusions and possibly increased depths of the surface
Tertiary sediments.
On the basis of an elementary concept of isostasy, the following equation
holds;
Bouguer Anomalies equal —gravitational attraction of the topography
—constant C {Marshall and Narain, 1954).
Assuming that the topography could be regarded as an infinite, level plane at
the altitude of the gravity station, we lave;
_ Bouguer anomalies equal —0-034 h —constant C.
The observed regression curve of Bougucr anomaly against elevation h for the
area investigated (Fig, 1) suggests that the following relationship holds:
Bouguer anomalies equal —0:0375 h —constant C.
This equation does not differ very much from the theoretical equation and this
then suggests that the general area is isostatically compensated in a regional
Sense.
The average Bouguer anomaly obtained for this traverse was —0-00112 gals.
and the average elevation approximately 456 ft,
The Bouguer anomaly values were then applied in yarious equations and by
graphical methods relating elevation and crustal thickness, and gravity anomaly
and crustal! thickness with the following results:
(1) Applying the equation relating gravity anomaly and crustal thickness
used by the Russian and Chinese scismologists, namely
H = 35(1 + tan h 90-0037 Ag)
where H is the crustal thickness and Ag the gravity anomaly, we obtain
H = 35(1 + tan h 0-0037(—1:1))
= 35(1 — 0-004L)
= 35 kilometres.
CRUSTAL THICKNESS MEASUREMENTS. SOUTIL EAST OF S.A, 35
(2) Applying the equation relating gravity anomaly and elevation used by
the Russian and Chinese seismologists, namely
II = 38 tan h(0-38 Ah — 0-18) + 38
where H is the crustal thickness and Ah is the elevation
H = 38 tan h(0-38 x 0:16 — 0-18) + 35
83 tan h(—0-12) + 35
—3-96 + 38 = 34 kilometres.
(3) Applying Andreev’s formula, namely
H = —0-1 Ag + 30
= —(0-1)(—1-1) + 30
= 80 kilometres.
(4) Applying Woollard’s graphical method relating depth of the Mohorovicic
discontinuity as a function of the Bouguer anomaly, we obtain a value of the
crustal thickness of 32 kilometres.
(5) Applying Woollard’s graphical method relating depth of the Mohoro-
vicic discontinuity as a function of elevation, we obtain a value of the crustal
thickness of 32 kilometres.
From these various methods an average value of 33 kilometres for the crustal
thickness is obtained. Now according to Cooke (1962) the average crustal
thickness for a region can be expressed in the form;
H = —62-9 + 0-485 Ag + 15-65 <V>
where <V> is the mean crustal velocity, Ag is the average Bouguer anomaly
and H is the crustal thickness.
Applying the values of 33 kilometres, and —1-1 milligals for HW and Ag,
we obtain a value for <V> of 6-16 kms/sec.
I I
REFERENCES
Cooke, 1962. Geophysics, 27 (6), pp. 892-897.
Dootey, J. C., end Wriuiams, L. W., 1960. Absolute gravity value in Adelaide. Aust. J.
Sci, 23, p. 17.
Hammer, Sicmunp, 1939, Geophysics, 4 (3), p. 184.
Hritanp, C., 1964. Exploration geophysical.
MARSHALL. and Nanam, 1954. Regional gravity investigations in the Eastern and Central
Commonwealth. U, of Sydney, Dept. of Geology and Ceophysics. Memoir 1954/2.
Mumm, I. A.. 1960. Absolute gravity determinations in Adelaide and recommendations for
a new permanent gravity base station. Aust. J. Sci., 23, p. 350.
Mumnrte, en 1963. Tectonic Evolution of the Mount Lofty Range Region. Aust. Jour, Sci.
26 (5).
AN AEROLITE FROM COCKBURN, SOUTH AUSTRALIA
BY J. E. JOHNSON* AND D. H. MCCOLLT
Summary
A small aerolite, found in deflated sandy country near Cockburn, on the New South Wales -
South Australian border, is described and classified as an olivine-hypersthene chondrite.
AN AEROLITE FROM COCKBURN, SOUTH AUSTRALIA
by J. E. Jounson® axn D, H. McCatrf
[Read 18 April 1967]
SUMMARY
A small nerolite, found in deflated sandy country near Cockburn, on the
New South Wales-South Australian border, is described and classited as an
olivine—hypersthene chondrite.
This meteorite was found during 1952 by the senior author on an aboriginal
campsite on Ophara Blocks Station (now abandoned), at a point where the
Cockburn-Egebek road crosses Ophara Creek. This is just inside New South
Wales (latitude 32°8°S.. longitude 141°4'E.) and is approximately six miles
southeast of Cockburn, South Australia. Hence, in accordance with the estab-
lished practice of naming meteorites after the nearest landmark te appear on
current survey maps, it has been called the Cockburn meteorite. The localit
is typical of many such aboriginal campsites, located in a region of low aad:
hills which in places haye been wind eroded, leaving a residuum of australites,
aboriginal artifacts, and indeterminate chaleedonic flakes probably also originat-
ing from aboriginal occupation.
DESCRIPTION
The meteorite has the form of a bipyramid based upon what was probably
a near-trapezoid shape, from which one corner has been recently broken away,
probably by aboriginals, so as to remove an estimated 20 per cent of the mass
of the meteorite, The length along the long diagonal of the trapezoid is 2-78
centimetres, the breadth when unbroken, across the short diagonal is estimated
to have been 2:0 centimetres, and the thickness between the apices of the
pyramids is 1-48 centimetres,
The faces of the steeper pyramid are all slightly concave, in contradistinc-
tion to those of the fatter pyramid which are convex, showing that the latter
was the anterior surface and the former the posterior during oriented transit
through the atmosphere.
The mass of the meteorite, prior to study, was 10-13 grams and when
entire it would have been little more than 12 grams, The overall specific gravity
is 3-47 which, although within the range for such meteorites, is rather low
indicating the weathering, that has taken place.
The surface bears the weathered remains of a fusion crust, now almost
entircly converted to limonite. The thickness of this crust varies from ()-1 to
1-0 millimetres, and is thickest over the convex anterior surface. Extent and
depth of weathering is further indicated by scattered warty excrescences of
deste Llu d ER” Scale Re! Pd Oe LR Se eS ee eer BOS
® Technical Assistanl, Mines Dept. of South Australia,
} Adelaide University, Geology Department.
Trans. Roy. Soc. 8. Aust. (1967), Val. 91.
58 J. E. JOHNSON ano D. HW. McCOLL
limonite up to 1-3 millimetres in diameter, through the fusion crust, These
seem where observable to coincide with underlying grains of troilite and/or
nickel-iron.
MICROSCOPIC
Transmitted Light: The meteorite is composed of an aggregate of grains
of olivine, orthopyroxene, plagioclase and opaques, The chondritic texture is
present although much obscured by. brecciation and recrystallisation. Weather-
ing has also stained the more permeable parts with limonite.
Olivine: Is present as clear colourless grains to the extent of 30 to 40 per
cent of the total. The composition of it estimated by X-ray diffraction measure-
ment of the 130 d-spacing is 25 = 3 mol, per cent of FesSiOx.
Orthopyroxene: Occurs as slightly turbid, often yellow stained grains com-
prising approximately 40 per cent of the total. The value of 2V was estimated
only with difficulty as between 60° and 70°, corresponding to 25 to 30 mol.
per cent. FeSiOs,
Plagioclase: Constitutes no more than 5 per cent of the meteorite. occur-
ring as colourless, clear, untwirmed crystals, filling spaces between the other
silicates, It has a very low refractive index, some orientations being less than
balsam, indicating it to be in the albite-oligoclase range.
Reflected Light: The opaque minerals are shown to be nickel-iron, troilite,
minor iron oxides (including chromite), und veins of secondary gocthite penetrat-
ing along zones of weathering. The nickel-iron shows regular graphic inter-
growths of kamacite and taenite (ie. plessita), indicating a nickel content of
10-15 per cent, which is typical of this class of meteorite. From this section,
which covered the entire cut face of the specimen, a micrometric estimation was
made of the percentage composition, counting at 20 micron intervals. This. gave
the following results.
Calculated
Percentage Percentage
(Area) by Weight
Silicates et # 89.14 §2.5
Nickel-iron w! as 3.87 83
Troilite _.. x a 5,45 7.1
Iron oxides ~ a 1.54 2.1
Total... 100.0
CONCLUSION
All evidence obtained concerning the composition of this meteorite places
it among the olivine-hypersthene chondrites (Classification of Mason, 1962),* the
most common classification of the acrolites.
That this stone may be related to the Silverton meteorite,? is a possibility,
as they are similar in composition and appearance. and were found abont twenty
miles apart, They differ only in degree of weathering and cohesion of consti-
tuent minerals, which effects may be related and consequent upon the sixty
years which intervened between their discoveries.
AEROLITE FROM COCKBURN, S.A. 39
ACKNOWLEDGMENTS
The authors wish to thank Dr. A. W. G. Whittle of the Adelaide University,
Economic Geology Department, for assistance in preparation of the microphoto-
graphs, and Mr. J. H. Biddle of the Adelaide University, Geology Department,
who carried out the X-ray diffraction measurements on the olivine.
The senior author gratefully acknowledges permission granted by the
Director of Mines for the publication of his observations on this meteorite.
REFERENCES.
1, Deer, W. A., Howie, R, A., and Zussman, J., 1962. The Rock Forming Minerals, vol. 1,
p.4
2. Mason, B., 1962. Meteorites, p. 91.
Spencer, L. J., 1934. A New Meteoric Stone from Silverton, New South Wales. Min.
Mag., vol. 23, pp. 569-572.
oe
J. E. Josnson anp D, H. McCoun PLATE 1
>
C
A. General view of Cockburn Meteorite. B. Thin section in polarised light to show chondrule
and silicate texture (x60). C. Polished section showing troilite (grey) and plessitic structure
in the nickel-iron (white) (x 250),
PARACANTHORHYNCAUS GALAXIASUS, A NEW GENUS AND SPECIES
OF ACANTHOCEPHALA FROM A FISH.
AUSTRALIAN ACANTHOCEPHALA NO. 12.
BY S. J. EDMONDS*
Summary
About 40 specimens of a fish Galaxias attenuatus (Jenyns) that were collected in some fresh water
streams and pools on the property of Mr. B. S. Hyde near Port Lincoln, South Australia, were
brought to me for identification by Dr. P. G. Martin of the University of Adelaide. The fish were
found to be heavily infested with acanthocephalans which differ from previously described genera
and species. If one uses Golvan's key (Golvan, 1960b: 713) they fall into the class
Palaeacanthocephala and the family Cavisomidae.
PARACANTHORHYNCHUS GALAXIASUS, A NEW GENUS AND
SPECIES OF ACANTHOCEPHALA FROM A FISH.
AUSTRALIAN ACANTHOCEPHALA No, 12
by S. J. Epmonps*
[Read 13 April 1967]
About 40 specimens of a fish Galaxias attenuatus (Jenyns) that were col-
lected in some fresh water streams and pools on the property of Mr. B. S. Hyde
near Port Lincoln, South Australia, were brought to me for identification by
Dr. P, G. Martin of the University of Adelaide. The fish were found to be heavily
infested with acanthocephalans which differ from previously described genera
and species. If one uses Golvan’s key (Golvan, 1960b; 713) they fall into the
class Palaeacanthocephala and the family Cavisomidae.
Paracanthorhynchus n,¢.
Diagnosis: Acanthocephala with characteristics of the subfamily Vanclea-
veinae Golvan, 1960a. Parasitic in small intestine of fresh water fish. Body
small, Trunk subcylindrical or fusiform. Body spines restricted to a small
triangular area on the anterior and ventral surface of the trunk. Arrangement
of body spines same in both sexes, Introvert of short to moderate length, cylin-
drical and with hooks that are not differentiated dorso-ventrally, Hooks with
simple rooting processes. Sheath double-walled and cerebral ganglion placed
in its middle. Lemnisci as long as or a little Jonger than the sheath. Male
organs occupy posterior half or two-thirds of the trunk, Testes ellipsoidal and
placed behind each other, Four cement glands, short and pyriform. Eggs
slender with polar prolongations of the middle shell. Type species: Paracan-
thorhynchus galaxiasus,
Paracanthorhynchus galaxiasus n.g., 0.8.p.: figs. 1-6
Small slender worms, ‘Trunk subeylindrical with maximum width in the
anterior third of worm. Body of preserved specimens may be straight hut body
of living specimens usually slightly S-shaped. Female noticeably Jarger than
male and the posterior part of its trunk mere slender.
Trunk: Length of male 2-7-4°2 mm and maximum width 0-5-0-6 mm;
length of female 4:5-8-0 mm and maximum width 0-5-0-9 mm, Srmiall triangular
area of body spines on anterior ventral region of trunk of both sexes, the spina-
tion scarcely extending to the dorsal surface of the trunk. Spines comparatively
large, 0-2-0°3 mm long. No genital spines.
Introyert: Cylindrical and not long, Length of armed section in male 0-32-
0-36 mom and maximum width 0-12-0-15 mm. Corresponding measurements. in
female are 0.32-0.38 mm and 0:13-0:18 mm. Unarmed truncated collar or neck
* Department of Zoology, University of Adelaide.
Trans. Roy. Soc. S, Aust, (1967), Vol. 91,
S. J. EDMONDS
lay
|
|
| \ YU
\
W
Figs. 1-6. Paracanthorhynchus galaxiasus. 1 male, 2 female, 3 introvert, 4 some hooks from
the introvert, 5 body spines, 6 eggs.
PARACANTHORHYNCHUS GALAXIASUS wn.st. 43
0-10-0-15 mm long, Armed with 12 rows of 7 hooks per row, the size and
shape of some of the hooks is shown in Fig. 4. Last hook of each row is smallest.
No marked difference observed in size of hooks on dorsal and ventral surfaces
of introvert,
Sheath: Arises just posterior to introvert hooks. Double walled, Length
about 0-6-0-8 mm and maximum width 0:19-0:23 mm. Ganglion present in
mid-region of sheath.
Lemnisci: Rather stout, about one to one and a half times as long as sheath,
Male structures: Testes, ellipsoidal, 0-35-0-45 mm long and in tandem.
Cement glands: Four, club-shaped and pressed closely together.
Male aperture: Appears to be subterminal in some but terminal in fully
extended specimens,
Female structures: Uterine bell about 0-4 mm long and uterus and vagina
about 2-0-2:5 mm long,
Eggs; Slender. Outermost covering very thin and collapses easily 55-67 »
long and 7-11 » wide with polar prolongations of the middle shell.
Type host: Galaxias attenuatus (Jenyns).
Type locality; Coomunga, near Port Lincoln, South Australia,
Holotype and paratypes: Australian Museum, Sydney.
Manter (1955: 67) reported the presence of acanthocephalans of the genus
Acanthocephalus from Galaxias attenuatus in New Zealand. Parasites of this
genus possess six cements glands and lack body spines. Consequently Manter’s
specimens must be different from the South Australian specimens.
REFERENCES
Gotvan, Y.-J., 19602. Le Phylum des Acanthocephala (troisiéme note), Arm. Parasitol.
35 (3), pp. 350-356.
Gotvan, Y.-J. 1960b. Le Phylum des Acanthocephala (troisitme note), Ann. Parasitol.
35 (5-6), pp. 713-723.
Manven, H. W,. 1955. Parasitological Reviews. The Zoogeography of Trematodes of
Marine Fishes. Exp. Parasitol., 4 (1), pp. 62-86.
SUBDIVISION AND STRUCTURE OF THE PRECAMBRIAN
(WILLYAMA COMPLEX AND ADELAIDE SYSTEM), WEEKEROO,
SOUTH AUSTRALIA
BY J. L. TALBOT*
Summary
The basement complex at Weekeroo can be subdivided into 6 major units of schists and gneisses.
Only one of these units shows undoubted sedimentary features although other of the units may be
sedimentary in origin. The basement complex has been deformed at least twice prior to the
deposition of younger Precambrian sediments. High grade metamorphism with associated
pegmatites and granites accompanied the first phase of deformation and a lower grade of
metamorphism appears to have been imposed in the second phase of deformation. The younger
Precambrian sediments consist of the Burra Group overlain unconformably by the glacial
Umberatana Group. The sediments and the underlying basement were deformed in the Palaeozoic
orogeny and metamorphosed to the biotite grade.
SUBDIVISION AND STRUCTURE OF THE PRECAMBRIAN (WILLYAMA
COMPLEX AND ADELAIDE SYSTEM), WEEKEROO, SOUTH AUSTRALIA
by J. L. Tausot*
[Read 13 April 1967]
SUMMARY
The basement complex at Weckeroo can be subdivided into 6 major units
of schists and gneisses. Only one of these units shows undoubted sedimentary
features although other of the units may he sedimentary in origin. The basement
complex has been deformed at least twice prior to the. deposition of younger
Precambrian sediments. High grade metamorphism with assuciuted peematites
and granites accompanied the frst phase af deformation and a lower grade of
Tavtamorphism appears to Have been iniposed in the second phase of deformation.
The younger Precambrian sediments consist of the Burra Group. overlain uncon-
formably by the glacial Umberatana Group, The sediments and the underlying
basement were deformed in the Palaeozoic orogeny and metamorphosed to the
hiotite prade,
INTRODUCTION
In the Olary region of South Australia two distinct sequences of Precambrian
rocks are exposed (Fig. 1), an older basement of schists and gneisses named
the Willyama Complex (Mawson, 1912) and younger Precambrian sediments
referred to the Torrensian and Sturtian Scries of the Adelaide System (Campana
and King, 1958), The Olary Province (Campana, 1956; Glaessner and Parkin,
1958) is one of a number of areas within the Adelaide geosyncline in which the
basement is exposed, The age of these basement outcrops is unknown but
granitic rocks within them have ages ranging from 1,700-1,400 million years
(Compston ef. al., 1966),
This paper describes the geology of a small area in the Olary Province.
Detailed mapping was undertaken to investigate the relationships between the
basement and overlying sedimentary mantle, The results of this mapping are
summarised in Fig. 2 which shows the distribution of rock units in the area
studied, A considerable modification of the rock units and structure reported by
Campana and King (op, cit.), is suggested as a basis for extension of the mapping
to other areas.
General Relationships
The distribution of rock types in Fig. 2 shows the younger Precambrian
Burra Group resting with marked unconformity on a folded sequence of schists
and gneisses. The structure in the Willyama Complex is dominated by a large
antiform® in the central outcrop and a series of antifurms in the western outcrop.
On the two simplifying assumptions that the units recognised in the Willyama
Complex reflect original sedimentary units and that the ventral antiform is in
A ih A Ee Sn I REA RN RS RSS RRS AARNE REY SNES
* Department of Geology, University of Adelaide. Present address; Department of
Geology. Lake ead University, Port Arthur, Ontario, Canada,
*"Campana and King interpreted this ventral untiform as a syncline and hence concluded
that the gneisses were younger than the schists. (Antiform is a duseriptive term for an arch-
like structure. It does not contain the stratigraphic implications of anticline, )
Trans. Roy. Suc, S. Aust, (1967), Vol. 91.
46 J. L. TALBOT
fact an anticline, a sucevssion can be erected for the Willyama Complex in which
the “leucogneiss” is the lowest and the “bedded mica schist” the highest recog-
nisable unit, Six mappable units have been recognised, their relationships being
shown in the map and legend of Vig. 2. A discussion of the validity of the
assumptions and hence the origin and significance of the rack units is given in
the final section of this paper,
Fig. 1, Locality Map. Area
mapped outlined in solid black,
north ef Mannahill.
Micrases Cua foe
_
i |
rOUNGEH (UTE CAMA AN ee
eo
The younger sequence occurs in four prominent tongues protruding into
the outcrop of the Willyama Complex. The structure of the tongues is complex
but the north-south trends are in marked contrast to the ENE trends of the
Olary Are in this general region. Explanations for this anomaly may he sought
in the relationships to the basement structures but such a discussion is beyond
the scope of this paper.
The Willyama Complex
The six nnits of the Willyama Complex consist of 4 lower units which are
essentially gneissic and 2 upper units which are schistose. Each unit is quite
variable but an attempt is made to describe the essential characteristies by which
the unit may be recognised in other arcas. The lowest unit is described first.
Layered and Foliated Leucogneiss
The lowermost structural unit is exposed in the core of the antiformal strue-
ture which dominates the southern central outcrop of the Willyama Complex.
The unit is composed of a Jower sequence of massive to macro layered leuco-
gneisses, granofels® and migmatites, a middle group of more migmatitic gneisses
and an upper series of layered gneisses. These layered gneisses show remark-
ably planar layering 1-10 cm thick and form a distinctive marker horizon. The
base of the unit is not exposed.
The mineralogical composition of the leucogneisses is simple, consisting
essentially of acid plagioclase with less quartz and with accessory lo minor pale-
olive biotite. Muscovite may also occur in minor amounts and some rocks with
a granitic appearance also contain microcline. The pegmatitic segregations in the
migmatites also show abundant microcline. The preferred oricntation of micas
is normally parallel to the layering but in the cores of some small folds is parallel
to the axial surface of the folds. The layering in the upper part consists of
alternations of plagioclase-quarty-minor biotite layers with coarser layers of
plagioclase-biotite with minor muscovite, (Plate 1, Fig. 1.)
* Granofels, Medium to coarse metamorphic rock with no obvious foliation (Goldsmith,
1959),
WiiiraM4s COMPLEN
Seddid mica sehist
AilWyiurm
YOUNGER PAECAMSSIAN
an Umberatone Group
F = ;
ara Gurra Grow
(GNEOQUS FOCwS
ey Afi phfonbe
. a
—1} Follated qrente
Mica schist a Bedding
Faotiatian
Laythsd ones ‘
Eroailei crass
Smull tovel
TT
om Cleavage
Mignal tic genial aall
—
Prue
(ones Leyeyane 53
Fig. 2. Simplified gealogic wap of yeirtivn wl Weekerar und Mtovialpa Stations, Sputh
Australia, The houndarles of the area are Lonpitudes 139° 455' to 139° 59°E ond
Luatitides 32* 10° to 32° 16'S.
45 J, L. TALBOT
Migmatitic Schist
Structurally overlying the layered gneiss is a quarts-feldspar-mica schist
crowded with pegmatitic schlieren. ‘The pegmatites are commonly only a few
centimetres wide, are lensoid and generally parallel to the foliation. Small
isoclinal folds in the pegmatites are common eyen in the cores of the large folds,
and a crenulation cleavage is developed parallel to their axial surfaces.
Compositional layering within the migmatitic schists is comparatively rare
aud where observed is thin and parallel to the cleavage, There are, however,
two bands of cale-silicate schists about 25 m thick which show well developed
layering. The layering in these schists conforms to the large scale structures,
the layering commonly being at a high angle lo the cleavage. The relationship
between the structures shown by the cale-silicate schists and the migmatitic
schists is shown schematically in Fig. 3. The layering in the migmatitic schists
is said to be transposed (e.g. Turner and Weiss, 1963, p. 94).
Fig. 3. Sketch showing the relationship
between the transposed migmatitic schist
unit (linvd) and gneiss band (stippled ).
The uppermost part of the migmatitic schist unit consists of a distinctive
layered biotite-gneiss 20 m thick,
In thin section the migmatitic schists show coarse relics of quartz, microcline,
muscovite and biotite in a highly foliated sericitic matrix. Plagioclase appears to
be uncommon in these schists but the presence of large amounts of sericite may
indicate that any original plagioclase may have been completely replaced. The
cale-silicate schists vary from layered two-mica schists to dark-brown biotite
schists with up to 80% cpidote. A blne-green hornblende and calcite occur in
some sections.
Granitoid Gneiss
Granitoid gneisses occur in the central part of the area and along most of
the eastern border, A wide varicty of rock types have been included in this unit:
weakly foliated granofels, gneissic migmatites, layered leucogneiss and some minor
schists. The lack of characteristic markers within this unit makes correlations
across faults and the delineation of macroscopic structures extremely difficult.
The gneisses along the eastern margin are particularly unsatisfactory in these
respects. A number of mappable sub-units can be distinguished in this area but
they are sufficiently repetitious to make it impossible to decide whether a major
structure corresponding to the central antiform is present in this region. Similarly
a definite correlation between these gneisses and those of the central region must
be regarded as tentative. An extension of the mapping to the east may solve
some of these problems,
SUBDIVISION AND STRUCTURE OF THE PRECAMBRIAN. WREKEROO, SA. 49
The mineralogy of the yneisses is relatively simple, quartz and plagioclase
(Au 15) being the most important constituents with smaJl amounts of biotite
and/or muscovite. Microcline occurs in some specimens and sphene and opaques
are ubiquitous accessories.
Layered gneisses and schists
In contrast with the non-layered nature of the previous unit the next highest
unit is layered on all scales. Macroscopic layering is clearly visible on aerial
photographs and is an expression of alternations of |eucocratic poorly layered
ancisses. with layered mica-gneisses and schists. The rocks are also well layered
on a small seale antl where sufficient biotite is present a foliation parallel to the
lithalogie layering is well developed. In a number of localities the more Jencn-
cratic phases of the gneisses grade laterally into dense, unlayered “aplitic” and
pesmatitic rocks, Campana and King (1958, p. 30) interpreted these changes
as a result of “blastic recrystallization” of pre-existing feldspathic rock.
The leucogneisses are composed of varying proportions of quartz and plagio-
clase with small amounts of K feldspar in some specimens. Trains of accessory
sphene, zircon and apatite commanly outline the only layering visible in the
tocks. Variable amounts of mica mav be present in the rocks and forms an
essential constituent of the schistose phases.
Miva Schist and Bedded Mica Sehist
The four units described above are predominantly encissic with some granitic
and minor schistose phases. Micas do not average above 20% in these units and
normally are considerably lower. In marked contrast to these gneisses is a group
of brown and grey mica-schists whicli crop out in the northern and western part
of the mapped Willyama Complex, These schists have been referred to as the
Weekervo-Schists by Campana and King (1958). In this study these schists
have been subdivided into a lower “Mica-Schist” unit and an upper “Bedded
Mica-Schist” and wre described separately. Campana and king (1958) rvcug-
nised an Ethiudna Cale-Silicate Group between the gneiss units already described
and these seltist units. The present author docs not recognise this as valid
regional unit for reasons to be discussed later.
Mieu Schists
The contact of the Weekeroo Schists with the structurally lower gneisses is
gradational. The thickness and number of Jeucogneiss bands decreases: rapidly
over a distance of 50 m to a dominant rock type of silky muscovite-rich schist,
Most of the “Mica Schist” outcrops are monotonous unlayered quartz muscovite
schists with muscovite commonly making ip over 50% of the rock, Some of the
outcrops contain abundant layers of quartz-rich schist which may be transposed
sedimentary layers, These layers ave however never sufficiently thick or persis-
tent to outline large scale structures,
‘The most common mineral assemblage of the schists is quartz-muscovite with
minur feldspar, biotite and/or chlorite, Garnet occurs in some specimens and a
light brown to blue pleochroic tourmaline is a common accessory, Some
localities show large white porphyroblasts with a tetragonal outline. Although
these porphyroblasts are now predominantly compased vf a white mica, relict
andulusite occurs in some, Rarely, slaurolite and chloritoid oceur within the
porphyroblasts and in one specimen sillimanite vecurred with them, No mutual
replacement textures were obscryed between these three minerals althoygh all
three appear to be replacing, the andalusite.
5) J. L. ‘TALBOT
Bedded Mica Sehists
To the north of the “Mica Schists” ave a sequence of schists and granofels
which show macrosopically folded layering visible on acrial photographs. The
macroscopic layering is parallel ta a small scufe layering which in places shows
ernss-bedded ripple structures (Plate 1, Fig, 2). There appears to be little
dowht therefore that the layering in this unit represents bedding. Consistent
fureset truncations indicate that the bedding and strictures north of the western
wiaphibolite are right way up, It is probable therefore that the “Bedded Mica
Schist" unit is younger than the “Mica Schist™ unit unless there is some
unsuspected structural complication,
The mineral assemblages of the bedded mica schists are similar to those in
the "Mica Schist" unit, Carnet and andalusite are however rare. The rocks are
finer grained and contain more quartz.
Older Precambrian Metamorphism and Igneous Activity
There are a number of metamorphic episodes affecting the Willyama Cam-
plex anc there are considerable problems in outlining a metamorphic history.
The general appearance of the rocks, especially the gneisses, suggests the meta-
morphic grade was quite high, Abundant migmatites, pegmatites and foliated
granites are suggestive of at least lower amphibolite facies. Relicts of sillimanite
and andalusite in the schists confirm this impression.
Most of the rocks however contain assemblages which are consistent with
the greenschist facies, that is, muscovite-chlorite-garnet in the schists and albite-
niuscovite in the gneisses, Tt appears therefore that an earlier phase of higher
grade metamorphism has been overprinted by a later phase of lower grade
metamorphism.
Structural evidence supports this hypothesis, and siuggests the second phase
of metamorphism occurred before the deposition of the Adclaide System rocks.
An early phase of tectonisin resulted in an essentially planar er at least isoclinal
attitude of layering with « foliation parallel to this layering. The large develop-
ment of migmatites and pegmatites also appear to be associated with this phase
of tectonism.
The pegmatites which are commonly parallel to the foliation vary in thick-
ness from a few centimetres to over LOO metres. The distribution of pegmatites
shows a high degree of correlation with rock type, pegmatites being most
abundant in the migmatitic schist and layered gneiss units and somewhat less
ahuntlant in the mica schist unit. On a smaller scale bands of mica schist und
cale-silicate schist within the migmatitic sehist unit are remarkably free of
pegmatite although the surrounding schists are crowded with pegmatites. Such
field occurrences suggest an intimale genetic rvlalionship between the formation
of the peginatites and metamorphism rather than an introduction af material
from outside. Such processes are typical of the middle of upper amphibolite
facies rather than greenschist facies.
The second phase of metamorphism is related Lo the sevond pluse of defor-
imation of the rocks in the Willyama Complex. This phase of folding has resulted
in the general outlines of the large scale structures now visible in the Willyama
Complex. The pegmatites are folded conformably with the lithologic layering.
During this phase of deformation most of the rocks were recrystallized and the
present mineral assemblages established, Most direct evidence of the previous
higher grade of metamorphism appears to have been obliterated during this
tectanie episode.
SUBDIVISION AND STRUCTURE OF THLE PRECAMBRIAN. WEKEREROO. S.A SI
The granites marked on the map (Fig, 2.) ave [pliated to some degree tut
differ from the granitic gneisses in their lack of marked compositional variation
across the bodies. The granites are composed of varying proportions of quartz,
microcline, albite, muscovite and hiotite. A weak preferred orientation of the
micas defines a poor foliation in some specimens.
The texture is coarse-grained hypidiomorphi¢ and the minerals show abus-
dant strain shadows in thin section, These textural features contrast strongly
with the unstrained granular texture of most of the gneisses.
Amphibolites are quite comipon fn the Willyvama Complex, the more immpar-
tant bodies being indicated in Fig. 2. Large amphibolites occur within the schist
sequences at several localities. The rocks are massive amphibole-slbite-epidote
rocks with no well pronounced foliation. Although metamorphosed, relict
igneous textures are common. It seems clear therefore that they represent altered
basic igneous rocks. Some structoral features are suggestive of a volcanic origin
(janes, Talbot and McBriar, 1962) but more recent work has brought to light
intrusive contacts and breccias and the racks are more reasonably interpreted
as dolerite plugs. Albitization of the surrounding country rock is also a
characteristic feature af these amphibolites.
Campana and King (op. cit.) interpreted these amphibolites as sedimentary
and equivalent to the Ethiudna Cale-Silicate Group. The present author, how-
ever, can find no evidence of sedimentary amphibolites in the Weekeroo area
although other types of cale-silicate occur within the migmatitic schist unit. An-
other group of dark green amphibolites occur as long, narrow nearly vertical
dykes generally with a north-south trend. In a nimber of localities the dykes
are folded on a large scale and in many places the margins of the dykes are now
chlorite schists with the foliation parallel ta the dyke margins, In some instances
the dykes follow faults. None of these dykes cut the Adelaide System rocks and
«a number of them are cut of by the unconformity.” The dykes, however, cut
across the large folds in the Willyama Complex and are therefore later than the
sevond phase of deformation. It is not known whether the dykes are related tu
the large amphibolite bodies but the generally massive nature of the latter
Suggests they were formed after the metamorphism associated with the second
deformation.
The Younger Precanibrian Metasediments
Lying with marked unconfonnity upon fhe Willyama Complex are meta-
morphosed sediments of the Adelaide System. Two sequences are represented,
x lower group believed to be the equivalent of the Burra Group (Torrensian)
and an upper group which is correlated with the Umberatana Group of Sturtian
age (for a discussion of correlations within the Adelaide Geosyncline sce
Thomsun, 1966).
The original sedimentary nature of the younger sequence of rocks fs readily
apparent. The rocks are well-layered and show an abundance of small scale
sedimentary features such as ripple marks, cross bedding and convolute lamina-
tions, and in the basal beds rare suncracks. Facies chanyes in manv horizons
gan be distinguished easily and original variations in the quartzites and ¢lactal
horizons are particularly prominent, The macroscopic structures are relatively
simple and individual marker horizons can be followed for comparatively large
distances.
* 4 single example of « light reen uralitized dolerite is seen cutting the folded Burra
Growp in the northeast tongue. This dyke has opt becn distinguished on the map froni the
Preeambrian amphibolite dykes but it is clearly later.
Jj. L. TALBOT
or
it
Many of the original sedimentary features, however, have been modified
by deformation and the overall simplicity of the large scale structures is some-
what misleading. Bedding in the schist units is largely subparallel to the foliation
and is heavily earsHcinel (Plate 1, Fig..3). Thinning of the schist units is also
readily apparent (Plate 1, Fig. 4) and so calculated sedimentary thicknesses are
unreliable, Tectonic thinning or thickening has not been. allowed for in con-
struction of the fence diagram in Fig. 4 so the thicknesses can only be regarded
as relative,
Burra Group
A generalised stratigraphic column for the Burra Group in the northeastern
seat is shown in Fig, 4. The relative positions of prominent marker beds in
the other three outcrop areas is also shown. Detailed columns could not be con-
structed in these other areas on account of poor outcrops. No attempt has been
made to subdivide the sequence into formations as the dominant rock type.
mica schist, is similar throughout the sequence,
Fig. 4, Stratigraphic column for
the Burra Gronp of the northeast
tongue (right hand pillar) and
fence diagram to show variations
over the whole area. The other
three uprights represent sections
inersured in the other three
tongues of the Burra Group. The
numbered marker beds are:— 1.
Basal conglomerate 2. Majar dolo-
mite 3, White quartzite 4, Cross
bedded silty sandstone 5. Sandstone
&, Tillite 7, Festoon ripple sand-
stone, Markers 1-4 are in the
Burra Group and 5-7 in the Um-
beratana Group.
The contact between the Burra Group and the Willyama Complex is well
exposed over most of the arca mapped and along all western contacts of the
Burra Group tongues is an unsheared sedimentary contact.
The rocks lying directly above the unconformity are for the most part meta-
morphosed conglomerates. In a few localities impure quartzites rest on the
Willyama rocks. The conglomerate is quite variable in particle size, composition
and thickness, and these variations show a correlation with variations in the
underlying Willyaia Complex.
The maximum thickness of the conglomerate is about 15 m and the maximnm
pebble size about 10 cm diameter. In general the thicker, coarser conglomerutes
are found in contact with the more schistose rock types of the Willyama Complex;
conglomerate may be absent altogether in contact with the more massive gneisses,
These differences appcar to represent lows and highs respectiycly in the
unconformity surface,
The composition of the basal beds varies sympathetically with the rocks in
the underlying Willyama Complex. In all the outcrops pebbles of vein quartz
are prominent. Adjacent to the gneisses, pebbles of quartz-feldspar gneiss are
very common and pebbles of quartz-feldspar-biotite gneiss are also. present,
Adjacent to the schists, gneiss pebbles arc less common and vein quartz pebbles
SUBDIVISION AND STRUCTURE GF THE PRECAMBRIAN, WEEKEHOO, 5A Bib
predominate, but as might be expected schist pebbles are not abundant. Pebbles
of amphibolite and albite rock are found in the conglomerate resting an the
amphibolite and in some exposures epidote (from the amphibolite) is abundant
in the matrix.
The conglomerate is interpreted asa reworked regolith, The correlation of
pebble type with underlying rock type in the Willyaraa Complex suggests that
there has been little transportation of the pebbles.
The higher beds of the basal unit consist of fairly uniform impure quattzites,
metagreywackes, minor conglomerates and interlayered mica schists. The quart-
zites commonly show cross-bedding, heavy mineral laminations, and ripple marks;
suncracks were observed in two localities.
Above this basal sequence the rocks are predominantly mica schists. The
most common mineral assemblage is quartz biotite-chlorite (muscovite) and
quartz-biotite-actinolite (dolomite, chlorite), Most of the rocks have a@ pro-
nounced preferred orientation of biotites although in many specimens a schistosity
is not obvious on casual inspection,
Tn the lower part of the sequence, bands of dolomite marble are commun,
and sedimentary magnesite occurs in some horizons. The must common assem-
blaves ave: quartz-dolomite, quartz-dolomitc-talc, The assemblage quartz-
dolomite-tremolite occurs in a number of localities.
Metasandstones are also common throughout the sequence, two prominent
horizons being a white ripple marked quartzite in the middle of the sequence
ani a fner grained impure sandstone near the top of the sequence. In the two
southern tongues a light grey quartzite with festoon cross-bedding occurs directly
beneath the Umberatana “tillite”.
Umberatuna Group
Rooks of the Umberatana Group rest with apparent conformity on the
Burra Group over much of the area but a distinct angular unconformity vf up
to 40° occurs in the northwestern part of the area, In this latter region the
Umberatana Group overlaps all parts of the Burra Group and rests directly on
the Willyama Complex, Where an unconformity cannot be recognised the base
of the Umberatana Group has been placed at tho first appearance of large
houlders in the schists, The incoming of large boulders also corresponds to a
general change in the appearance of the mica schists, 1n contrast with the schists
of the Burra Group which are soft and show a good schistosity, the schists of
the Umberstana Group are hard dense brown rocks commonly with only a
poorly developed schistasity.
The basal unit of the Umberatana Group, interpreted as a tillite by Campana
and King (op. cif.) is a quartzrich biotite granofels with large boulders and
with hedding completely absent in most outcrops. The horizon is very variable,
containing numerous large boulders in some parts and being almost free of
boulders in other parts. The boulders range in size up to 50 em diameter and
are most commonly well-rounded, althongh boulders less than 5 cm diameter
tend to be sub-angular. The composition of the boulders is very variable. in
some outcrops boulders from the Willyama Complex are dominant, whist im
others dolomites and quartzites from the Burra Group predominate. The matrix
of the “tillites’* is a characteristic dark grey structureless fine-grained biotite
* The sedimentary term. “tillite” is used to describe this rock as no sutistactory meta-
morphic term is available, 7
54 J. i. TALBOT
granofels which no longer shows sedimentary characteristics. Orginal grains
larger than 0-1 mm are however still preserved, These grains, mostly of quartz
but also of aggregates of dolomite or quartz (and feldspar) vary from rounded
to sub-angular and shew a wide variation in grain size. The reconstituted matrix
in which these fragments occur has a gtain size varying from 0-02-0-05 mm and
consists essentially of quartz, olive-green biotite and carbonate, with accessory
muscovite and granular opaqnes.
The rocks above the basal “tillite” are dominantly fine-grained quartz-rich
mica schists and granofels with minor dolomite marbles and quartzites. Scapolite
occurs as porphyroblasts up to 0°5 cm in diameter in some horizons in the mica
schists in the northern part of the area. Scattered boulders (most commonly
granite) up to one metre in diameter occur in all parts of the sequence but
are wacommon in the upper part. Sedimentary structures, such as convolute
laminations and small scale crass-hedding, are common in the quartz-rich mica
schists.
In contrast to rocks of the Burra Group, biotite shows a rather poor pre-
ferred oricntation in the Umberatana Croup rocks, with a consequent lack uf
foliation in most outcrops. This lack of foliation is net regarded as a fundamental
metamorphic difference between the two groups but rather due to differences in
lithology,
Palagozoic Metamorphiym and Igneous Acticity
The mineral assemblages in the Adelaide System rocks are indicative of
biotite grade (middle greenschist facies) of metamorphism. No granitic rocks
or pegmatites are found within the Adelaide System rovks and the only evidence
of large scale metamorphic differentiation is the presence of quartz veins in some
localities. Quartz in pebbles and in quartzites show strong preferred orientatiuns
which are related symmetrically to the axial plane schistosity (Talbot, 1962).
The metamorphism and large scale folding and deformation appear therefore to
be related and correlation with the major orogeny which affected the whole of
the Adelaide Geosyncline, indicates it to be Palaeozoic in age.* A single light
green dvke occurs cutting the folded Burra Group NNW from the Weekerou
Station shearing shed. The rock is naw largely an assemblage of albite, chlovite,
epidute and magnetite, showing relict lathes of plagioclase. It therefore appears
that this dyke was intruded after the peak of the Palaeozoic metamorphism and
certainly after Folding had ceased.
Structural History
A detailed analvsis of the structural geology is beyond the scope of this
paper and only a brief outline of the structural history will be presented here.
As noted previously the overall distribution of rock types within the Willy-
ama Complex is largely the result of the second recognizable tectonic event,
This period of deformation affected rocks which already possessed a well defined
schistosity and which were already high grade metamorphic rocks, that is,
gneisses and migmatites, Large scalc folds were formed with a new foliation,
a crenulation cleavage, parallel ta the axial surface. The trend of this steep
foliation is roughly NE to ENE and the associated large scale folds commonly
plunye ut moderate angles to the NE although a wide range of plunises has been
observed. The majority of the amphibolite dykes were intruded after this phase
of deformation and it is alse pessible that the large amphibolite bodies were also
formed at this time.
* Latest information suggests the age of the metamarphism of the Adelaide Geosyncine
rocks is 490 m, years, (Campston et. al., 1966.)
SUBDLVISION AND STRUCTURE GF THR PRECAMBRIAN. WEEKKEKOO, S.A. 35
The younger Precambrian sequence was deposited on the already multiple
deformed Willvama Complex. Some movements must have occurred after the.
deposition of the Burra Group but the next major tectonic episode is the lower
Palaeozoic orogeny which affected the whole Adelaide Geosyncline. ‘he major
trends of this Palacozoic folding in the Olary region are ENE-WSW but highly
divergent trends ate apparent in the vicinity of the areas of basement outcrop.
Only minor inodifications of the fold patterns in the Willyama Complex have
vecurred during the Palaeozoic orogeny but a number of large vertical slip
faults have altered the distribution of rock types.
Nomenclature and correlation
The area mapped appears to be critical to a discussion Of the stratigraphic
relationships in both the older and younger Precambrian, Cumpana and King
(op. eit.) recognized Four main groups of rocks. in the Willyama Complex, namely
“Archaean Mctusediments As”; “Feldsputhised Archagan Metasediments AF;
“Migmatites and Granite Gneisses Am” and “Anatectic Granites. Granodiorites
and Granulites Ag”. The last group docs not uceur in the areca mapped anil is
not discussed further, Campana envisaged the first three units as representing
different stages of granitization vf similar sediments and his map shows cores of
Am surrounded by zones of Af and finally As, although a number of important
exceptions do occur (e.g. near Old Boolcoomata Homestead ).
The “metasediments” were divided into a lower group (Weekeroa Schists)
a Middle Group (Ethindna Cale-silicate Croup) and an Upper Croup (Qutalpa
Arkosic quartzites passing to granite gneisses)" (Campana and King, 1938,
p. 21), The Ethiudna Group is said to occupy “a well defined stratigraphic
horizon within the schistose succession”. The relationship between the “Weekeroo
Schists” and the “Outalpa quartzites” can be seen in a number of localities, eg.
Weekcroo, Old Boolcoomata and Ameroo Hill, where schists are in contact with
eneisses, the wantuct being: parallel to the layering in the gneisses. The middle
or Ethiudna Group is shown by Campana to lie within the schist sequence in
all localities shown on the map except in the type locality of Ethiudna Mines.
In this locality, near Plumbago Ilead Station, the group consists. of cale-silicates
untt dolomites in an isolated gneissic terrain whose “stratigraphic” position is
unknown. ‘The “stratigraphic” position of the Ethiudna Group as the Middle
Croup of metasediments is however determined by the position of amphibolites
at Weekeroo, Amuroo Lill and Old Boolcoomata, In none of these localities do
the rocks resernble the Ethiudna rocks and in fact in two of them the cale-silicates
are intrusive igneous rocks. In addition, cale-silicates occur in other parts of the
section (e.g. in the migmatitie schist unit at Weekeroo) and it is considercd
unwise to make long range correlations of this sort in gneissic terrains,
It is therefore proposed that use of the term Ethiudna Calc-silicate Group
us a regional unit be discontinued.
The remaining rock types in the Weekerou section were grouped by Cam-
pana and King inlo “Migmatite and Cranitic Gneiss unit Am” with the genetic
implication that they are more altered than the “Archacan Metasediments As”.
These have heen subdivided in this study into 3 units which are recognised as
part of the overall sequence and not as more metasumatized rocks,
* On Campana’s map of the Weekeroo region this unit is inched with the: “Miematites
and Granitiy Gneisses Am”, imstead of with the “Metasediments As", This ix ¢learly a
dratting error.
1
Plate
TALBO'U
L.
5G J. Li. ‘TALBOT
A comparison of Campana and King’s units and the units proposed for this
study is shown in Table 1. The sequence proposed for this paper is not neces-
sarily a sedimentary sequence althougli many of the rocks are sedimentary in
origin. The origin of the layering and of the boundaries of the gross lithologic
units is of special importance to this problem. In all the schist units except
the hedded mica schist unit, layering, whether originally sedimentary or not, is
now heavily transposed parallel to the second generation cleavage. Hence strati-
graphic relationships within these units have been completely destroyed, Never-
theless, the gross relationship between the major lithologic units has not been
profouudly altered by this second phase of deformation which resulted in the
large scale folds now visible in the Willyama Complex.
TABLE 1
Wallies Conepler Sequence
Sequence of Informal secuence
| Carmmpana & King (1958)* inverted uacd in this Paper
r | Bedded mica schist.
“Archaea” Weekerog schist |
| Mies. Schist
Meiasediments 4 |
Ethiudna Cale-Silicate Group |
{As} L Outalpa Quartzitest | Layered gneiss
r Granituid gneiss
Migmatites
und 4 Unditterentiatedt Miguiatitie schist
Granite-Gneisses
(Ant) L N Leucogneiss
* Campana's sequenre has been inverted as the evidence from the presint study suggests that
the selusts are the youngest part of the Willyaria. Complex sequence,
+ This umt is called “Arkosie Quartzites, Passing to Granite-CGneisses” in the text (Campana &
King 1958 p.18) but is referred to hy name in the map legend and also in Cumpana (1957).
¢ This unit was not recognised by Campana ass “stratigraphic unit but aa rocks ma particular
alate of alteration,
In contrast to the schist units the more massive gneissic units show relatively
little transposition parallel to the new cleavage and even where folded show a
foliation parallel to visible layering in the rocks, (Exceptionally a new foliation
is developed in some rocks parallel to the axial surface uf smull folds.) In the
more massive gueisses the foliation is discontinuous or defined by a preferred
orientation of micas. In the layered gneisses foliation is well developed in the
mica rich portions and is invariably parallel to the layering, In the quartzo-
feldspathic layers trains of accessory minerals such as zircon and sphene are
observed parallel to the gross lithological layering,
The evidence suggests that although the foliation is parallel to layering the
presence of layering is not a necessary condition for the formation of the
foliation, Jt seems unlikely therefore that the foliation represents a simple
“bedding plane foliation” imposed on relatively undisturbed planar bedding. It
is more likely that the gneissic units have been heavily deformed and that the
parallelism of foliation and layering are the result of large scale isoclinal folds
with possibly large amounts of transposition on a small scale. This phase of
SUBDIVISION AND STRUCTURE OF ‘TILE PRECAMBRIAN, WEIEKEHOO. S.A, 57
deformation resultect in an essentially planar attitude of layering and foliation
and was accompanied by high grade metamorphism and the formation of
peymatites. This planar layering was then folded by the second phase of
deformation to give the observed major folds,
The suceession of units in the Willyama Complex may not therefore have
any stratigraphic significance (with exception of the bedded mica schist. This
init appears anomalous in the general contest of the Willyama Complex and it
was entertained that there could be an uncontornnity between it and the remain-
ing units, No direct evidence could be found to support this suggestion ),
The present study confirms the recognized stratigraphic relationships of the
uverlying Adelaide System. Campana emphasized the transgressive nature of
the Umberatana Croup and in the Weekeroo area an angular unconformity
between the Burra and Umberatana Group is now well established. Recent
mapping by the 5,A, Mines Department has demonstrated this unconformity in
many other parts of South Australia, Differences of interpretation however arise
with structure and metamorphism. The differences in structural interpretation
are of limited interest but the failure by Campana to recognise the metamorphism
in the Adclaide System rocks may lead to an incorrect assessment of the economic
»otentialities of the younger group of rocks. Kecognition that the rocks have
seen Metamorphosed to the biotite grade also removes some of the limitations
to the tectonic interpretation of the area, and also imposes strict limitations to
age determinations in the Willyama Complex,
REFERENCES
Casmana, By 1956. Granites, orogenies and iineral genesis in the Olary Province (South
Australiu). Jour, Geol. Soe, Aust, 4. pp. 1-12.
Campana, B., abd Kawa, D.. 1958... Regional Geology ancl Mineral Resouces of the Olary
Provinve, Geol, Surv, S Anst. Ball, 84, 133 pp.
Comms'ros, W., Craawron, A. K,, and Bormann, V. M., 1966. A Radiometric Mstimuate of the
Duration of Sedimentation im the Adelaide Geosyneline, South Australia, Jone, Geol.
Soc, Avst., 13, pp. 229-276,
Gruaesyver, M, F., and Panes, L. W. (dy) (958. The Genlngy of South Australia.
Jonr, Geol. Soc. Aust, 5 (2). 163 pp.
Co tosmin Ry 1959. Granofels. a new metamorphic rock name, Jour, Geol, 67, pp. LOO-1 10,
Jonws, J.B. Tatuor, J. L., and MoBnian, E. M.. 1962. A suite of voleanie rocks with apilitic
affinities from the Archaean of South Australia, Aust, Jour, Sei, 29, p. 356,
Mawson, DM, 1912, Geological Investigations in the Broken Hill Area, Mem, Roy, Soc,
5. Aust. 2, pp. 24 1-310,
Tatsor. J, L.. 1962, A study of the structural and inetamorphic relationships between Older
and Younger Preeambrion rocks in the Mount Lofty-Olary Are, South Australia. Unytrbl.
Thesis, U. of Adelaide, 171 pp.
Thomson. B, P,, 1966. The Lower Boundary of the Adelaide System and Older Basement
Relationships in South Australia, Jour, Geol. Soe, Aust. 13. pp. 203-228,
Yourner, F, J. and Wess, L. E., 1963, Structural Analysis of Metunorphic ‘Tectonites,
MeGraw-Lhill.
EXPLANATION OF PLATE
Phare |
Mig, 1. Banding in yneiss tear Lop of Jeuvogneiss amit, Lal, 32° 13-7'S Long, 138° 5608's,
Vig. 2. ‘Vruneated laminations and scour anc fl strneture in uranofels of the bedded mica
schist unit. Lat, 32° 12-65 Long. 139°" 54°,
Fie, 8. Transposed layering in the wppermost beds of the Burra Groop. Arrows point to
Fold closures, Lat, 32° 10-5’S Long, 139° 58-1'F.
Fiv. 4, Bulk strain of the Umbpratana Tillite as indicated by deformed dolomite: erratics.
100 metves N of locality of Plate 1, Fig, 3.
PHERETIMA TUMULIFACIENS (OLIGOCHAETA, MEGASCOLECIDAE)
A NEW SPECIES OF EARTHWORM FROM THE SEPIK DISTRICT, NEW
GUINEA
BY K. E. LEE*
Summary
Pheretima tumulifaciens, a new species of earthworm, belonging to the family Megascolecidae, is
described. It was found in the Sepik River Valley, northern New Guinea, where it is associated with
unusual forms of micro relief that have been attributed to the earthworms’ burrowing and casting.
The species is most closely related to P. sangirensis (Michaelsen), from Indonesia, but in some
respects resembles Megascolex. The inadequacy of generic distinctions and of the criteria for
distinction of groups of genera are discussed.
PHERETIMA TUMULIFACIENS (OLIGOCHAETA, MEGASCOLECIDAE)
A NEW SPECIES OF EARTHWORM FROM THE SEPIK DISTRICT,
NEW GUINEA
by K. E. Lee’
[Read 8 June 1967]
SUMMARY
Pheretima tumulifaciens, a new species of earthworm, belonging to the
fanily Megaseolevidae, is deseribed. Tt was fund in the Sepik River Valley,
northern New Cuinea, where it is associated with unusnal forms of micro-
relief that have been attributed to the earthworms’ burrawing and casting. The
species ig inost closely reluted to P, sdngirensis (Michaelsen), from Indonesia,
hut in sone respects resembles Megascolex. The inadequacy of generic distinc-
tions and of the eriteria for distinction of groups of genera are discussed.
INTRODUCTION
Haantjens (1965) recorded micro-relief in the form of irregular pits,
trenches, mounds and ridges, not unlike some periglacial phenomena, from the
humid tropical grass-covered plains bordering the Sepik River valley, south of
Wewak, in New Guinea. Populations of a large earthworm species were always
associated with the micro-relief and Haantjens (1965) considered that they were
responsible for the formation of the micro-reliet features.
In October, 1965, the author visited four sites in the vicinity of Yangoru,
where Haantjeus had observed micro-relief features, to collect carthworms and
examine the relationship between thcir activities and the micro-relicf features
attributed to them, At each of the sites, large earthworms belonging to an
undescribed species of Pheretima Kinberg were collected. The earthworms
were Closely associated with the micro-relief features, as recorded by Haantjens,
but it seemed unlikely that they were directly responsible for the micro-relief,
A discussion of the micro-relief features and their possible origin will be pub-
lished elsewhere (Lee (in press)). The large earthworm associated with the
micro-relief features has heen named Pheretima tumulifaciens, and is described
below.
Pheretima tumulifaciens n.sp.
Collection Data. (1) About 14 mi S of Kworo Village, 20 mi SW of Yangoru,
District, New Guinea; 0-33 em in soil under kunai grassland; 2 clitellates; K.E.L.
29/10/65. (2) About # mi SW of Watibi no. 2 Village, 15 mi SW of Yangoru;
0-30 em in soil under secondary forest; | aclitellate; K.E.L. 22/10/65. (3) About
1 mi N of Watibi no. 2 Village, 14 mi SW of Yangoru; 0-53 cm in soil at edye
of deep trenches, under kunai press ans 1 clitellate; K,E.L. 22/10/65. (4)
About 1 mi SW of Haripmor Village, 15 mi SE of Yangoru; 0-45 cm in and
under low mounds and ridges covered by kunai grassland; 6 clitellates; K.E.L.
93/10/65.
* Division of Soils, C.S.1.R.0., Adelaide.
Trans. Roy. Soc, §. Aust, (1967), Vol. 91.
au K. E. LEE
Type Material. Holotype and two syntypes lodged am South Australian
Museum.
Dimensions. Mature specimens are 500-600 mm in length, 9-10 mm in
diameter (in ethyl alcohol) and have 550-600 segments. Detailed measurements
of the holotype are: Length 590 mm; segments 587; diameter 10-5 mm at_vii,
9-5 mm at xiii, 9-5 mm at clitellum, tapering gradually tu 6 1mm at about half
length and fairly uniform to posterior end. Posterior to iii the segments have
secondary annulations, two to five per segment.
Colour, Pale greyish-brown with pale brownish-red clitellum.
Chaelae, Absent on i, otherwise ahout 140 per segment, evenly spaced on
a slight ridge around cach segment, nearer the anterior than the posterior margin
of the segraents; without a mid-dorsal gap, but with a small mid-ventral gap,
about twice the nermal chactal interspace; a few chaetae missing immediately
adjacent to each male pore, oa xviii, and across the mid-ventral line adjacent ta
the female pores, on xiv.
Prostomium prolohous.
First dorsal pore at 10/11,
Cliteluunm covering entire body surface from slightly posterior to the chaetal
ring on xiii to the line of the chactal ring on xvil,
Spermathecal pores: one pair. at 7/8, each on a prominent, transversely
elongate papilla, about 2 mm x 1 mm, the pores each about 8 mm from the
ventral mid-line,
Female pores: one pair of smal) pores on xiv, about 0-75 mm apart. one
each side of the ventral mid-line, surrounded by a pale elliptical area, in line
with the chaetal ring.
Male pores: ventral on xviii, one on each side, each about 3-5 mm from
ventral mid-line, in line with chaetal ring, not on papillae; each pore medial to
a deep longitudinal groove, oyerhung by a prominent ventro-lateral ridge that
runs longitudinally from xvii to xix (Iigs. 1, 2),
Tubercula pubertatis: two pairs of prominent, flattened papillae, a pair on
xvii and 4 pair on xix, each papilla about 3 mm diameter, forming, together with
the prominent ventro-lateral ridges on xviii, the edges of a deep depression that
becupies the ventral surface of xviii (Figs. 1, 2).
Sepla v/vi, vi/vii, vii/vili and viii/ix are thickened and strongly muscular.
Thick muscle fibres arise from the body wall in segments vi-ix and rm forward
to an insertion on the posterior surfaces of the muscular septa; some of the fibres
are atlached anteriorly to the pharynx and not to the septa, Similar muscles
have been observed previously in many earthworms, especially in large species;
their purpose is apparently to produce unusually powerful contractions of the
anterior segments, probably to facilitate burrowing and provide the traction
necessary to move the large bulk of the carthworm'’s body. In most species of
Pheretina, septa viii/ix or ix/x, or both of them, are absent or greatly reduced in
size. This is not so in P. tremilifaciens.
The pharynx occupies most of i-iv, and has a diffuse glandular coating, with
many fine muscle fibres attached to the body wall. In v-vii the alimentary
canal is a thin-walled tube with large finely lobate salivary glands lying, beside
it and opening by narrow ducts into the pharynx. Giszard strongly muscular,
in viii. Ocesophagus extends from ix to xv where it expands abruptly into the
intestine, close to the anterior end of xv, There is no typhlosole. Many species
of Pheretima have a pair of rounded or conical intestinal caeca, arising in xvvi
PHERETIMA TUMULIFACIENS, NEW EARTHWORM SPECIES
Fig. 4
vibv.
Fig. 1. Pheretima tumulifaciens, ventral aspect, segments xiii-xx.
Fig. 2. P, tumulifaciens, diagrammatic transverse section at segment xviii,
to show position of male pores in relation to ventro-lateral ridges.
Fig. 3. P. tumulifaciens, arrangement of hearts of segment xiii in relation
to dorsal and ventral blood vessels (diagrammatic ).
Fig. 4. P. tumulifaciens, left prostate, medial aspect.
Fig. 5. P. tumulifaciens, left spermatheca, medial aspect.
ABBREVIATIONS
cl, = clitellum; d-b.v. = dorsal blood vessel; div. = spermathecal diverticulum; f.p. =
female pore; h, = heart; lr, = ventro-lateral ridge; m-p. = male pore: pd. = prostatic duct;
uct;
p.gl. = prostatic gland; sac = spermathecal sac; sp.d. = spermathccal
sp.p. — sperma-
thecal pore; t.p, = tuberculum pubertatis; v.b.v, = ventral blood vessel.
fi2 KE. LEE
ov thereahouts, and projecting ferwurds, sometimes through several segments,
usually pressed tightly against the ventro-lateral ov lateral aspects of the intestine.
There are no such caeca in P. tasmelifactens.
Dorsal Wood vessel unpaired; it can be traced forward to the posterior end
of the pharynx, where it divides into several branches, Stout commissural
vessels (hearts) in x-xiii, one pair in each segment, connecting the dorsal and
ventral blood vessels; the two vessels of cach pair have a short transverse con-
nection across the oesophazus, independent of the connection of the two vessels
to the dorsal vessel (Big. 3), There is no independent supra-intestinal vessel
connecting the hearts lonyitudinally. In vii-ix similar lateral vessels arise from
the dorsal vessels, but divide into a oumber of brauches leading to segmental
organs aed are not “hearts”. The testes are in x, xi; those of xi are in testis sacs
that occupy much of the coelomic cavity in the segment, Ovaries in xiii, One
pair of small, racemose resiculae seminales, in ix. Prostates in xviii, one on cach
side; laminar glandular portion with branching duets, all discharging into a
short, stout, strongly muscular prostatic duct (Viv. 4). Spermathecue in viii,
one pair, each discharging through a thick, rauscular duct at the anterior murgia
of the segment; the sac is cylindrical, a little wider than the duct, projecting
backwards into the segment and set of from the line of the duet; a cluster of
sinall diverticula opens into the duct close tu its junction with the sac (Fig. 5),
Micronephridia arc small and numerous in cach segment, irregularly scattered
over the peritoneum,
DISCUSSION
P. tumulifaciens differs from most species of Pheretima in having well-
developed, strongly muscular septa in the segments adjacent to the gizzard, a
characteristic shared with many large megascolecid earthworms, especially
those which, like P. tumulifaciens, make extensive burrow svstems going Lh to
considerable depths. In most species of Pheretima the anterior septa are not
thickened and septa viii/ix or ix/x or both of these are absent, or much reduced,
The absence of intestinal caeca also distinguishes P. tumulifaciens from many
other species of the genus. The only character that decisively places this species
in Pheretima is the position of the gizzard, in viii. If the gizzard were in v, vi,
or vil, it would be placed in the genus Megascoelex, There is need for a thorough
re-examination of the criteria on which generic distinctions in megascolecid
earthworms are based. Revised groupings of genera have been proposed by
Gates (1959), Lee (1959) and Omodeo (1958). The proposed new groupings
are hdsed on slightly different bases, but none of the proposals has contributed
greatly to the improvement of the state of confusion that has developed over
the years since Michaelsen (1900) and Stephenson (1930). defined the genera
amd grouped them into sub-families and families on the basis of a supposed
“family tree" of generic relationships, derived from a study of only a few
anatomical characters. Sims (1966) has attempted to clarify the relationships
between genera, using a computer tu assess the affinities of 30 species, belonging
to 29 megascolecid genera, on the basis of 43 attributes of each species. The
results of his study favoured the scheme of classification proposed hy Gates
(1959) for taxonomic categorics above the leyel of genera, Computer tech-
niques may take a useful contribution to megascolecid taxonomy, as they make
it possible to assess relationships on the basis of a larger number of attributes
than can be handled by traditional taxonomic methods. However, if computer
techniques are to be used, it is at the Jevel of definition of genera that they can
ephaely contribute most, and Sims’ study assumes that the zenera are adequately
efined.
PHERETIMA TUMULIFACIENS, NEW EARTHWORM SPECIES 63
P. tumulifuciens shows closest affinities to P. sangirensis (Michaelsen), an
Indonesian species. Similaritics and differences between the two species are
summarised below.
P. tumutlifaciens P. sangirensis
Spermathecal pores 1 pair, at 7/8 1 pair, at 7/8
Female pores paired, close to Ventral unpaired, median
mid-line ventral
Septum viii/ix present, muscular present, membranous
First intestinal segment XV xv
Intestinal caeca absent sometimes present,
very short
Vesiculae seminales 1 pair, in ix 2 pairs, in xi, xii
Spermathecal diverticula cluster of small diver- 1 ellipsoidal
ticula diverticulum
REFERENCES
Gates, G. E., 1959. On a Taxonomic Puzzle and the Classification of Earthworms. Bull.
Mus, Comp. Zool., Harv., 121, pp. 229-61,
Haantyens, H. A.. 1965. Morphology and Origin of Patterned Ground in a IIumid Tropical
Lowland Area, New Guinea, Aust. J. Soil Res., 3, pp. 111-29,
Lez, K. E., 1959, The Earthworm Fauna of New Zealand. N.Z. Dep. Sci. Industr. Res.
Bull., 130, pp. 1-486. Govt. Printer, Wellington.
Ler, K, E. {in press). Micro-relicf Features in a Humid Tropical Lowland Area, New
Guinea, and their Relation to Earthworm Activity. Aust. J. Soil Res.
MicHAELseN, 1900. “Oligochaeta.” Das Tierreich, vol. 10, Berlin.
Omonro, P., 1958, Le réserve naturella integralé du Mont Nimba. I. Oligochétes. Mem.
Inst. Fr, Afr. Noire. 53, pp. 9-109.
Sims, R, W,, 1966, The Classification of the Megascolecoid Earthworms: an Investigation
of Oligochaete systematics by Computer Techniques. Proc. Linn. Soc, Lond., 177 (2),
pp. 125-41.
SrepueNnson, J.. 1930. “The Oligochaeta.” Clarendon Press. Oxford.
PERMIAN DEPOSITS OF SOUTH AUSTRALIA AND THEIR FAUNA*
BY N. H. LUDBROOK}
Summary
Lower Permian sediments occur in all the main sedimentary basins of South Australia. The Cape
Jervis Beds are described, and the Lake Phillipson Beds and Stuart Range Beds formally named.
In general, the formations follow a sequence of boulder clay overlain by sands and clays mostly of
marine origin, with a widely distributed fauna of arenaceous foraminifera of which Hyperammina,
Ammodiscus, and Hemidiscus are the most common. Twenty-three species, of which four are new,
are recorded or described. The most varied fauna occurs in the Stuart Range Beds from which the
gastropod Peruvispira was recovered.
PERMIAN DEPOSITS OF SOUTH AUSTRALIA AND
THEIR FAUNA*
by N. H, Lupsrooxt
[Read 8 June 1967]
SUMMARY
Lower Permian sediments ocenr in all the main sedimentary basins of
South Australia, The Cape Jervis Beds are described, and the Lake Phillipson
Beds and Stuart Range Beds formally named. In general, the formations fallow
a sequence of boulder clay overlain by sands and clays mostly of marine orixin,
with a widely distributed fauna of arenaceous foraminifera of which Fyper-
ammina, Ammodiseus, and Hemidiscus are the most common, ‘l'wenty-three
species, of which four are new, are recorded or described. The most varied
fama occurs in the Stuart Range Beds from which the gastropod Peruvispira
was recovered,
INTRODUCTION
As recently as 1955, Permian sedimentation in South Australia was 50 im-
perfectly known as, on a map of Australia showing regions of Permian sedimen-
tation (Hill, 1955), to be restricted to glacial deposits in a southeast-northwest
trough south of Adelaide, extending from Encountcr Bay to western Yorke
Peninsula. While this is still recognized as the main area of outcropping Permian
glacigene sediments, Lower Permian sands and clays have been proved by
exploratory drilling to occur widely in all the main sedimentary basins. More-
over, as reservoir beds for nafural gas accumulation in the Great Artesian Basin,
Permian rocks have assumed an economic importance not foreseen a decade
ago (Sprigg, 1966).
Until foraminifera were discovered in the Permian section of Minlaton
Stratigraphic Bore (Ludbrook, 1956), the depositional environment of most of
the Permian sediments in South Australia was inisunderstood, It was generally
believed that the sandy nature of most of the deposits indicated a Auvio-glacial
origin, and that “Huvio-glacial depositions in ponded waters are but rarely met
with in our Permo-Cayboniferous strata and marine depositions of this age are
entirely absent” (Mawson, 1926). The ubiquity of foraminifera in the Lower
Permian in all the main sedimentary basins, except that part of the Great Artesian
Basin, including the Cooper's Creek Sub-basin, occurring in the northeast of
the State, disproves this helief,
Alter initial over-deepening by ice, marine incursions in fjords or narrow
troughs took place in two main and widely-separated areas following the general
southeast-northwest trend. The southeastern area includes the Murray and St.
Vincent Basins and the northwestern area the part of the Great Artesian Basin
lying | between the Peake and Denison Ranges, Stuart Range, and Margaret
Creek.
* Published with the permission of the Director of Mines.
} Senior Palaeoutologist, Geological Survey. of South Australia.
Trans. Roy. Soc. S. Aust. (1967), Vol. 91,
66 Nv. TI. LUDBROOK
Localities from which Permian marine sediments have been proved in
surface sections or by drilling are shown in Fig. 1.
All material and figured specimens are housed in the collections of the
Geological Survey of South Australia, except those lent by the Geology Depart-
ment, University of Western Australia (UWAGD).
133
3 Vy
NORTHERN | ————__,_ TERRITORY | QUEENSLAND
a ene ei
Boorthanna
(Duff Creek)
Stuart Range—>
*eCoober Pedy
Lake Phillipson “, sfo4oje
s
5/641/6 Coorie Appa
j Railway: LAKE
' TORRENS
| Nullarbor, No.8 LAKE
GA/RONER
ore «
| WALES
Ls
ho
t
\
NEW SOUTH
Monash ;
«Pon ess
Minlaton a Renrerk
Stansburyfs ADELAISE |
Trowbridge Shoal 7 Clayton j
Cape Jervis 4 a
LOCALITIES WITH PERMIAN
FORAMINIFERA— Second Valley
MILES 50
Km 8¢
Fig. 1. Map showing localities with Permian foraminifera.
ST. VINCENT BASIN AND ADJACENT AREAS
Since Selwyn’s recognition in 1859 of glacial features in the valley of the
Inman River, there has accumulated a considerable volume of descriptive litera-
ture on the Permo-Carboniferous or Permian glaciation and glacial deposits in
PERMIAN DEPOSITS OF S.A, AND FAUNA a
the St. Vincent Basin and adjoining areas to the east on Fleurieu Peninsula and
io the west on Yorke Peninsula. The papers of Howchin (1926) and Campana
and Wilson (1955) may be consulted for historical reviews and comprehensive
lists of references,
Without designating any standard section, Howchin described most if not
all of the known exposures of Permian deposits in the arca between Adelaide
and Kangaroo Island. ‘The sequence at Hallett Cove he referred to as the
“Hallett’s Cove beds” (1895, p. 65), while the glacigenes of Inman Valley were
variously designated “Inman Valley Shale” (1895, p. 68) and the “Inman River
Beds” (1926, p. 102). Unfortunately, neither of the names Hallett Cove nor
Inman is now available for stratigraphic purposes as they have been applied
to other units.
The most complete ontcropping sequences described by Howchin are those
at Hallett Cove, Cape Jervis (David and Howchin, 1897) and King’s Point,
near Victor Harbor (1910a). Of these David and Howchin recognized the
section at Cape Jervis as “the most extensive development of glacial till that
has been up to the present observed in South Australia” (1897, p. 64). The
section was iJlustrated hut not redescribed by Campana and Wilson (1953, 1955),
The Cape Jervis exposure is here deseribed by R. B. Wilson and the writer
as the holostratotype section of the Permian deposits of St. Vincent Basin and
the adjoining areas:
Cape Jervis Beds (Fig. 2).
Type Section: Jervis 1-mile geological sheet,
On coast, patenting for one mile (1-609 km.) northeast of Cape Jervis
Lighthouse, Hundred of Yankalilla, sections 212, 211, 3009, 3010.
Thickness; 95 feet (29-87 m.).
The Cape Jervis Beds are unconformable upon easterly dipping greywackes
of the Cambrian Kanmantoo Group. They are overlain by kunkar. The type
section is described as follows:—
Thickness
Unit Lithology feet metres
6 Poor outcrop, grass covered slopes, probably clay as below,
boulders on surface _ 23°5 7-2
5 Clay shele—grey-brown, fissile. gritty with scattered boulders,
becoming red-grey motiled toward top a Ae 53 29-5 9-0
4 Sandstone—yellow-white, cross-bedded. with scattered cal-
careous pebbles Ka . x ; “i 7 i 5 15
3. Sandstone—gritty sandstone and prit with boulders and thin
interbeds of laminated fissile grey clay ‘m 7 be 13 3-9
2 Till-dark grey boulder till with clay-shale bands os bs 5 15
1 Till-sandy till with boulders of all sizes, principally Kan-
mantoo yreywacke and Victor Tarbor Granite. ‘Thin
asia (6 inches to I foot; 0-15— 0-3 m,) limestone bands... 22, 6-7
B
"Total measured thickness of Cape Jervis Beds unconformubly
overlying Cambrian Kanmantoo Group 2 os 98 29°8
The fossil locality number is 5/837/2 Gervis 2). The grey clay and over-
lying red and grey gritty clay of bed 5 are tossiliferous, arenaceous foraminifera
being present in samples CJ, 7 and C.J. 8. Abundant tests of Recurveides
wilsoni Ludbrook sp. nov. accompanied in decreasing order of abundance by
68 N. H. LUDBROOK
Hyperammina coleyi Parr, Ammovertella huwchini Ludbrook sp. noy,, Digitina
recurcata Crespin and Parr, Ammodiscus oonahensis Crespin and Hyperammina
acicula Parr.
The Cape Jervis Beds are extensively developed on Jervis and Yankalilla
l-mile sheets.
WwW E
SCALE O 40 80 FEET
ie] 12:1 242 Metres
Pig. 2. Sketch of type section of Cape Jervis Beds, Cape Jervis.
A southerly view of the Cape Jervis section showing the Cape Jervis Beds
(C.J.) overlying Kanmantoo greywacke (K) is shown on plate 1, figure 1. Fig,
2 illustrates. the lower part of the section to the sandstone ledge at 40 feet (12
m.) above the base; the interbedded nature of the sandstone and olay and the
tendency for the boulders to he bedded in some parts of the section is also
shown at the position of the hammer. Fig. 3 illustrates the dip ( probably
depositional) and bedding of the same part of the section as figure 3, viewed
south. Fig. 4 is that of a striated boulder on boulder clay at the most northerly
end of the exposure.
The Cape Jervis Beds are very subject to gully erosion which is illustrated in
plate 2, figure 1 of the northern part of the exposure.
The section at Cape Jervis provides confirmatory evidence of marine incur:
sion in the Adclaide region following initial overdeepening by glaciation in the
late Carboniferous to early Permian. Previously a tew broken fragments of
Hyperammina. were recovered from clay collected by B. P. Thomson from Second
Valley (locality Jervis 1, 5/837/1), but no other foraminifera had been observed
in Permian glacigenes between Adelaide and Kangaroo Island.
Parastratotype sections of the Cape Jervis Beds are exposed at Hallett Cove
where the formation rests on striated pavements now declared a national reserve,
and at King’s Point west of Rosetta Head, on Encounter Bay, where the sequence
PERMIAN DEPOSITS OF 3.4. AND PAVNA 6y
of moraine, glacial till, and sandstone described and illustrated by Howechin in
1910 is still undisturbed (plate 2. figure 3),
At Selwvn's Rock (plate 2, figure 2) the southern bank of the Inman River
has recently heen considerably eroded at the position of the large erratie in
leoulder clay overlying the striated pavement.
Exposures, however, nowhere attain any great thickness, and Permian sedi-
mentation in the Adclaide region consists for the most part of infilling of over-
deepened glacial valleys and basins as those of Fleurieu Peninsula (Campana
and Wilson, 1953, 1955) and Kangaroo Island where a bore at Kingscote in
1909-1910 intersected 950 feet (289 m.) of typical Permian sequence before
bottoming in slate. Leaf impressions were collected in 1953 by R. C. Sprigg,
then of the Geological Survey of South Australia, in Permian sediments three
miles (4-8 km.) southwest of Penneshaw, Their fragmentary nature preclu
identification at the Australian Museum other than that they were possibly
portions of equisitaean stems.
In the St. Vincent Basin and adjoining areas only the Jower part of the
Permian sequence uppears to be represented. The absence of coals and of good
microflora-bearing clays demonstrates that the Artinskian and upper part uf the
Sakmarian are missing in this area, On the other hand, the occurrence of Per-
miun megaspores in the lower Tertiary of the St. Vincent Basin suggests that the
ahsence of the upper part of the sequence may be due te erosian rather than t
nun-ceposition,
The Permian is 776 fect (236 m,} thick on Yorke Peninsula where it provides
the clay pans for the salt lagoons which are exploited for commercial sult pro-
duction. The sequence was completely intersected in Minlaton and Stansbury
Bores (Ludbrook, 1966a). In Beach Petroleum Troubridge Shoal No, 1 Strati-
raphic Well, 750 feet (225 m.) of Permian sediments were cut between S90
eet and the total depth of the well, Foraminifera cccurring sporadically
hetiveen 1,010 and 1,550 feet (307-8 and 472-4 m.) permit close correlation with
the marine interval in Stansbury Bore, Here also the upper Sakmarian-
Artinskian earbonaccous sediments are absent.
MUMNRAY BASIN
Presumed Permian glacigene sediments were proved by drilling im the
Murray Basin in South Australia at Renmark, Monash and Clayton. A.O.C,
North Henmark No. 1 entered at 3,245 feet (989 m.) blue-grey boulder clay
irregularly interbedded with calcareous sandstone in irregular lenticles and
laminae. Slump structures were common, while erratic pebbles and grains of
quart, granile, «rey metamorphic rocks and dark pink feldspar were variously
scattered throughout the groundmass. Faceted pebbles were recovered al 3,431
feet (1,045 m.). At 3,788 feet (1,154 m.) (Core 15) there was a calcareous
pyritic quartz sandstone, and at 3,864 feet (1,184 m.) (Core 16) blie-grey shale
irregularly interbedded with lenses of calcarcous sandstone containing pink
feldspar, biotite and pink garnet. The well bottomed in sandstone with scattered
coal fragments and conglomerate bands, small slump structures and swirls of
fine clay, Foraminifera occurred in almost all the cuttings between 3.410 and
4,000 feet (1,039 and 1,219 m.), but as none were recovered from cores their
persistence does not necessarily indicate marine environment for the lower part
of the interval.
To N. J. TUDAROOK
Similar sedinents with a few foraminifera were intersected in Beach Petre.
leun Monash No, L Well between 2,930 and 3,820 feet (493 and 1,011 m.). ‘Ihe
formation was conglomerutic at 3,285 feet (1,001 m.).
A considerable thickness of at least 1,600 feet (487 m.) of Lower Permian
sands and shale was intersected in W.G. Goyder Donna No, 1 Well drilled ai
Clayton, 54 miles south-southwest of Milang, near the southwestern murgin of
the Murray Basin. At 500 feet (152 m.) the well passed into brownish mud-
stone with fine muscovite and some carbouaceous matter, This was a thin hed
uverlying pyritic sand with subanyular to subrounded quarty. and pink garnct
grains, grading to sandstone and sand with some interbeds of fine-grained cal-
careous sandstones, The quartz grains were more or less rounded, with pitted
surfaces; pink garnet was common und pyrite usually present with accessvries
of muscovite, feldspar and lithic grains. A few foraminifera, cither Anwnodiscus
or Hemidiscus, were present in most samples between 540 and 1,050 feet (164
ancl 320 m.).
Without the evidence of foraminifera these sediments would be regarded
as “fluvio-glacial”. In Donna No. 1 Well there is less evidence of boulder clay.
while the sands for the most part are worn and of reasonably uniform size. The
section therefore corresponds to the Lower Sakmarian. marine sediments in the
Yorke Peninsula bores. Owing to drilling difficulties good bottom cores were
not ubtained to prove the base of the sequence,
Sediments of possible Permian age with a species of Trochammina not
known from other Permian sediments in South Australia occur below 255 feet
(77 mm.) in a water bore at Blackford on section 500, Hundred of Murrabinna.
GREAT ARTESIAN BASIN
Western Part — Lake Phillipson and Boorthanna Troughs
Following the recognition of 2,000 feet of Permian sediments in Lake
Phillipson Bore (Balme, 1957), the sequence of Lower Permian rocks inder-
lving the western part of the Great Artesian Basin, was described by Ludbrook
(1961), und the history of their deposition and geological sctting reviewed by
Woptner (1964). The Lake Phillipson and Boorthanna Troughs between Lake
Phillipson and the Peake and Denison Ranges contain the most complete
suecession identified hy Balme as Sakmarian-Artinskian, consisting in upward
sequence of a maximum of 2,974 feet of glacial till and boulder clay, marine
mudstanes and siltstones, overlain by Glossopteris- and Gangamopteris-bearing
Freshwater silts and clays with sandstone and coal interbeds now descrihed
from the Arckaringa Sub-basin as the Mount Toonudina Beds (Freytag, 1965),
All but the uppermost coul beds were recently intersected between 490 fect
(149 m.) and the total depth of 2,048 feet (623 m.) in Stuart Rance No. 3 Hore,
drilled by the South Australian Mines Department in search of additional under-
ground water supplies for Coober Pedy Opalficld. The marine formatiun below
the Mount Toondina Beds in this well provided the most significant fauna xo far
recovered from the South Australian Permian, Stratigraphic, Wthopical, and
palacontological details of this well are in press (Ludbrook, 1967).
Except for the Monat Toondina Beds, the Permian sediments in the Lake
Phillipson and Boorthanna Troughs have not been formally named. Balme
(1964) informally used the names “Lake Phillipson Coal”, “Lake Phillipson
Glacials”, in tabulating the stratigraphic pusitiun of pre-Tertiary micro-loras,
and the names “Coober Pedy Beds” and “Stuart Range Beds” on a locality snap
of Permian localities frou which palynological data were available. Tt is hore
PERMIAN. DEPOSITS OF S.A, AND FAUNA 7
propused to formalize the names Lake Phillipson Beds for the glacigenes al
the base of the sequence and Stuart Range Beds for the mudstones and silt-
stones, marine in part at least, between the glacigenes and the Mount Toarnidina
Beds, using Lake Phillipson Bore (Ludbrook, 1961) as the standard subsurface
section.
The Lake Phillipson Beds ave so named to avoid further duplication of
stratigraphic names for the glacigene boulder clays or till at the base of the
Permian sequence. It is recoguized that the boulder beds ocvur in outcreps on
the Oodnadatta and Warrina 1:250,000 sheets from which a type section might
he selected to comply with the Australian Code of Stratigraphic Nomenclature.
The relationship of these auterops to the Lake Phillipson Beds or to the Crown
Point Formation of the Northen Territory is not, however, firmly established.
Scattered oeeurrences of Permian(?) tillite were briefly described and mapped
in the Peake and Denison Ranges west of Mount Dutton, 45 miles (7-2 Kim.)
north-northeast of Warrina, three miles (4-8 km.) northeast of Duff Creek Siding
and three miles (4-8 km.) northeast of Box Creek Siding (Reyner, 1955).
In the standard section, the Lake Phillipson Beds occurring between 2,337
feet (718 m.) and 3,140 feet (957 m.) overlie granite basement and consist of the
sequence already described (Ludbrook, 1961) of 783 feet (238-7 m,) of grey
boulder clay with some limestone and calcareous sandstone,
The Lake Phillipson Beds were intersected in Stuart Range No, 3 Bore
between 1,660 feet (505 m.) and the total depth 2,043 feet (623 m.) in which
the formation consisted of 100 feet (80:4 m.) of pinkish sandstone with scat-
tered coarse quartz grains, red feldspar, pyrite, biotite, pink garnet, granite
pebbles and 283 fect (86:2 m.) of boulder conglomerate with granite and other
boulders of heterogeneous rock types.
The formation was also intersected in Coorie Appa anil Margaret Creek
Bores (Ludbrook, 1961).
The Stuart Runge Beds overlie the Lake Phillipson Beds. So tar they have
not been recognized in outcrop, They are 1,613 feet (491-6 m.) thick between
744 feet (226-7 m.) and 2,337 feet (715 m.) and were described ( Ludhrook,
1961) as a sequence of 88 feet (26-8 m.) of bluce-grey mudstones with foramini-
fera, overlain by 1,525 feet (464-8 m.} of sandstones and siltstones. Only the
lower nit in Lake Phillipson Bore appears to contain foraminifera.
The Stuart Range Beds are well distributed in the Coober Pedy-Stuart
Range area of the Lake Phillipson Trough and in the Boorthanna Trough. ‘They
were intersected between 910 feet (277 m.) and 1,660 feet (505 m.) in E. & W.S.
Stuart Range No, 3 Bore where they contained an abundant and persistent
fauna of foraminifera with rare molluscs, ostracodes and vertebrate remains.
They are represented in samples of grey clay collected from spoil from three
bores on Balta Baltana Station on Billa Kalina 1;250,000 sheet, Bulta and Ware
l-mile sheets. The depths at which the Stuart Range Beds were intersected are
net known accurately, but they are known to underlie the Lower Cretaceous
Marree Formation, Jealities of the bores Balta Baltana No. 1 (Ware 5,
5/641/5), No, 2 (Ware 3, 5/641/3), No. 3 (Balta 6, 5/640/6) are shown on
Map 8 Billa Kalina (Ludbrook, 1966b). All contained foraminifera which were
abundant at locality 5/641/5. In the Boorthanna Trough the beds appear te
attain their greatest thickness of 1,903 feet (580 m,) in Beorthanna (Duff
Creek) Bore, thinning out to the south to 240 feet (75 m.) in Coorie Appa
Bore and rapidly disappearing to the east of a line hetween Boorthanna, Anna
Creek and Coorie Appa.
72 MN. , LUDRROOK
it may be anticipated from seismic data (Moorcroft, 1964; Freytag, 1965)
and the Permian isopach map of Kapel (1966) that over 3,000 feet (914 m, } of
similar sediments occur in the Arckaringa Sub-hasin southwest of Oodnadutta
and north of the Boorthanna Trough.
Northern South Australia: Simpson Desert
Lower Permian sections were intersected in two wells, Witvherrie No, 1
and Purni No. 1 of French Petroleurn Company (Australia) Pty. Ltd., located
in the north of South Australia on the southern margin of the Simpson Desert.
The sequence consisted of an upper unit 41 fect (12 m.) thick of dark
shale with coal and a lower unit consisting of 290 feet (88 m.) of sandstone and
shale and 241 fect (80 m.) of siltstone and shale with quartzite pebbles (Canaple
and Smith, 1965). The upper unit which has been compared with the coal
sequence in Lake Phillipson Bore presumably belongs to the Mount Toondina
Beds, while the lower unit is regarded by Canaple and Smith as equivalent to
the Crown Point Formation.
Northeastern Sauth Australia: Cooper's Creek Sub-basin
In the Permian of the Cooper's Creck Sub-busin tu the northeast of South
Australia gas discoveries have been made on the Gidgealpa and Moomba struc
tures. The sequence of three disconformably transgressive units has been
named (Kapel, 1966) the Gidgealpa Formation.
The Permian sediments were described by Greer (1965) as. sandstones,
lignitic shales and coals which accumulated in alternating coastal swamps,
brackish lagoonal and shallow-water marine environments, In Gidgealpa No. |
Well, the Permian is “underlain by 400 feet of Permo-Carboniferous marine
shales and sands”, Kapel (1966) subdivided the Gidgealpa Formation into
three subunits; a lower of sandstone, shale and coal; a middle of shale, siltstone
and minor coal; a top subunit of sandstone minor shale and coal. Wopfner
(1966) divided the Formation into a lower Permian unit of conglomerate ant
sedimentary breceia in black or dark grey silty matrix, and carbonaceous shale
interbeds, and an upper Permian unit of light grey fine- to very coarse-grained
sandstone, dark grey carbonaceons shale and coal seams.
‘the Formatiou therefore has yet to be formally defined. The highly esr-
honaceous nature of most of the sequence is in contrast to the low carbon contett
of the light grey claystones and sandstones containing foraminifera which occur
over the boulder clays elsewhere in South Australia.
Upper Permian carbonaceous siltstone, silty sandstone, conglomerate and
arkosie crossbedded sandstone with coal and plant remains were intersected in
Delhi-Frome-Santos Innamincka Nu, 1 Well in the northeast of the State.
EUCLA BASIN
Knowledge of Permian sediments in the Eucla Basin is limited to the single
becurrence of Artinskian [ossiliferous clay in Nullarbor No, 8 (Yangoonabie)
Bore (Harris and Ludbrook, 1966).
FAUNA AND AGE OF THE PERMTAN DEPOSITS
The fauna contained in the Cape Jervis Beds, the Stuart Range Beds, and
their equivalents, is sparse, indicative of a restricted environment of low tem
peratures or low salinity. With two exceptions, the faunal assemblage consists
PERMIAN DEPOSITS OF S.A. AND FAUNA 73
only of 23 species of arenaceous foraminifera, of which species of Hyperammina,
Ammodiscus, and Hemidiscus are the most common and ubiquitous. Hippo-
erepinella biaperta Crespin and Reophax thomasi (Crespin) are distributed in
small numbers in all the sedimentary basins; Lagenammina ampulla (Crespin )
and Glomospirella nyei Crespin are restricted to the Lake Phillipson trough;
Thuramminoides sphaeroidalis Plummer, Ammovertellina (?) glomospiroides
Ludbrook sp. nov., Glomospira adhaerens Parr, Tolypammina undulata Parr,
Recurvoides wilsoni Ludbrook sp. nov., are well distributed frequently in abund-
ance, As the foraminiferal fauna is almost entirely endemic it provides no
ieliable basis for correlation. Thurammrinoides sphaeroidalis described from the
American Pennsylvanian is known to have a range of Middle Silurian to Permian,
while (?)Hyperammina expansa (Plummer) was described from the Middle
Pennsylvanian Strawn Group of Texas.
The most significant fossil so far recovered is the gastropod Peruvispira in
Stuart Range No, 3 Well at 1,285-1,305 feet. This genus, known only from
Lower to Middle Permian marine rocks, confirms the Permian age of the Stuart
Range Beds determined by Balme (1957) from microforal evidence. In
Stuart Range No. 3. Well the single specimen of Pertuvispira was associated with
a fragment of ? Contlaria. Other sparse elements of the fauna include astra-
cndes and vertebrate remains which have not been identified.
SYSTEMATIC DESCRIPTIONS
Order FORAMINIFERIDA
Superfamily AaMopisCACRA
Family ASTRORHIZIDAE
Subfamily RaizaMMiINNAE
Genus Hiepocrerinetca Heron-Allen and Earland, 1932
Hippocrepinella biaperta Crespin
pl. 3, fig. 1
1958. Wippucrepinella biaperia Crespin, 37, pl. ¥. figs. 1-18.
Description, Test free, broadly clangate, consisting of a single tube open at
both ends, sides parallel, ends constricted, the greatest constriction towards the
aperture which is surrounded by a more or less thickened lip, aboral end open,
less thickened when it is preserved, but usually broken off;, wall thick, wrinkled,
agglutinating, consisting of quartz grains in a siliccous matrix,
Dimensions. Hypotype F£379, length 1-05, width 0-25 mm.
Type Locality. Oonah, Tasmania; Quamby Mudstone.
Material. Hypotype G.S.S.A. F£379;, 51 specimens.
Distribution. Minlaton Bore, Stuart Range No. 3 Bore, Fossil localities
Ware 5 (5/641/5) and Balta 6 (5/640/6), Nullarbor No. 8 Bore, A.O.C. North
Renmark No. 1 Bore,
Stratigraphic Range. Lower Permian.
Subfamily HirpocREPINnINAE
Genus HypexamMMina Brady, 1878
Hyperammina acicula (Parr)
pl. 3, fiz. 7
1942, Hyperamminuidey acicula Parr, 105, pl. 1, figs. 4, 5; pl. 2, fig, 4,
1958. Hyperammina acicyla; Crespin, 44, pl. 5, fig, 11; pl. 6, fig. 7 (xynonyrny ),
74 N. Ui. LAUDBROOK
Hyperammina acicula is a large tapering species with a thick smoothly
finished wall with much cement. Fragments only have heen recovered in South
Australia, but they compare with paratype material.
Dimensions. Holotype length 11 mm., greatest diameter 1-3 mm., paratype
on UWAGD slide 20767 length 11 mm., greatest diameter 1-2 mm.; the figured
hypotype GSSA._ F£370 is only L mm. long.
Material. UWAGD 20767 five paratypes, 20770 three paratypes, 20771 one
paratype, 20772 four paratypes, 195 fragments in South Australian samples,
Distribution. Stansbury and Minlaton ores; locality Balta 6 (5/640/6),
Boorthanna, Coorie Appa and Stuart Range No, 3 Bores: Goyder Donna No. 1
Bore; Nullarbor No. § Bore.
Stratigraphic Range. Lower Permian.
Hyperatmina coleyi Parr
pl. 3, firs. 89
1942. Hyperammina coleyi Parr, 104, pl. 2. fig. 3; 1958, Crespin. 46, pl. 6. figs. 5, 6; pl. 7,
figs, 3-5; pl. 33, figs. 1-2.
Hyperammina coleyi is a large species with a subglobular proloculus and
a slender tubular chamber of lesser diameter than the proloculus. The wall is
thick, firmly but not smoothly cemented as in H, acicula; the surface is rough.
Dimensions, ‘The type series ranges in length to 9 mm.,, the proloculus
diameter ()-5-l mm., tubular chamber diameter 0-5 mm. Figured hypotype
GSSA F¥371 proloculus diameter 0-55, diameter of tuhe 0-45 mm.
Material. UWACD 20766 three paratypes, 20769 one paratype, 20770 two
paratypes, 20771 four paratypes, 20772 one paratype; 100 fragments in South
Australian samples.
Distribution. Cape Jervis; Stuart Range No. 8, Stansbury and Nullarbor
No. 8 Bores.
Stratigraphic Range. Lower Permian.
(?) Hyperammina expansa (Plummer)
ph. 3, fig, 10
1945. Wyperamminoides expansus Plinmer. 223, pl. 16, figs. 1-8,
1958. Hyperammina expansa: Crespin, 49, pl. 4, figs. 9-12,
Short flaring specimens with a thick wall and apparently wide aperture in
undamaged specimens belong to the species referred hy Crespin (1958, p. 49)
to Hyperamminoides expansus Plummer, As the genus Hyperamminoides has
been synonymized by Locblich and Tappan (1964) with Hippocrepina, and
Conkin (1961, p. 261) has noted similarities between H. expansa and the micro-
spheric form of Hyperammina casteri Conkin the specific identification and
affinities of the Australian species must remain in doubt.
Dimensions of Figured Specimen. Height 0-4, diameter 0-4 mm.
Type Locality. Algerita, Texas, U.S,A,; Strawn Group. Middle Pennsy)-
vanian.
Material, Hypotype GSSA F372; 11 specimens.
Distribution. Stansbury, Coorie Appa, Stuart Range No, 3 and AOC North
Renmark No, 1 Bores.
Stratigraphic Range. Middle Peunsylyanian; ?Lower Permian.
-1
ct
PERMIAN DEPOSITS OF S.A. AND FAUNA
Hyperammina hebdenensis Crespin
pl. 3. figs. 2-6
1958. Myperemmina hebdenensis Crespin, 52, pl. 6. figs. 8-12,
Description. Test free, small, broad, straight, consisting of a globular
proloculus followed by a nearly straight tubular second chamber; wall agglu-
tinating, moderately thin, with fine quartz grains in much cement. ‘The cement
is usually siliceous but some specimens have calcareous cement. Aperture a
large circular opening at the end of the tube.
Dimensions. Hypotype GSSA Ff375 length 0-75, proloculus diameter 0-25;
hypotype GSSA F376 length 1-26, diameter 0-6 mm.
Type Locality. Hebden, N,S,W., Mulbring Subgroup.
Material. 526 fragments.
Distribution. Ubiquitous in South Australian material.
Stratigraphic Range. Lower Permian.
Observations. Vt is not always easy to distinguish H, hebdenensis from
H. coleyi when they usually occur as tubular fragments. In this study the two
have been differentiated by the wall thickness with relatively little cement in
coleyi; the smaller size, relative smoothness of the wall finish and the fact that
the tube diameter is only a little less than that of the proloculus in H, hebdenensis.
Family SACCAMMINIDAE
Subfamily SaccamMMrmNinaE
Genus LacenAMMinA Rhumbler, 1911
Layenammina ampulla (Crespin)
pl, 3, fig. 14
1958, Pelosina ampulla Crespin, 42, pl. 2. figs. 1-3.
Description. Test free, consisting of a single Hask-shaped globular chamber;
wall agglutinating, consisting of very ine quartz grains in much siliceous cement;
aperture usually oval, terminal, at the end of a short neck.
Dimensions. Hypotype length 1-00, width 0-5 mm.
Type Locality. Oonah, Tasmania; Quamby Mudstone.
Material. Wypotype GSSA F£387, 7 specimens.
Distribution. Locality Ware 5 (5/641/5), Stuart Range No. 3 Bore.
Stratigraphic Range. Lower Permian.
Observations. Conkin (1961, p. 248) noted the obscurity of the affinities of
Proteonina Williamson, 1858, Lagenammina Rhumbler, 1911, and Seccammina
Sars, 1869. Pelosinu ampulla Crespin possesses the diagnostic features of
Lagenammina rather than those of Pelosina as it has been redefined by Loeblich
and Tappan (1964, p. C200).
Genus Saccammina M. Sars in Carpenter, 1869
Saccammina orca Ludbrook sp. nov.
pl. 3, figs. 11-13
Description. Test free, large, solid, consisting of a single globular chamber
of somawhat variable shape; it is commonly barrel-shaped with irregular annular
constrictions but may be flatly spherical without apertural neck, or Hask-shaped
with a broad neck; wall thick, consisting of an inner pseudochitinous layer and
76 N. JI. LUDBROOK
an outer layer of quartz grains held together by calcareous cement; extcrior
roughly finished; aperture oval, usually without neck, but may be at the end
of a broad, short neck.
Dimensions. Holotype F384 length 1-8, diameter 1-1; paratype Ff385
length 1-15, diameter 0°75; paratype Ff386 length 1-2, diameter 1-1 mm.
, Type Locality. E, & W.S, Stuart Range No. 3 Bore, 1,305 feet 8 ins.-1,327
eet,
Material, 368 specimens,
Distribution. Stansbury Bore; locality Balta 6 (35/640/6), Boorthanna, Lake
Phillipson, Stuart Range No, 3 and Nullarbor No. 8 Bores.
Stratigraphic Range. Lower Permian,
The specific name is taken from the Latin noun urca, a jar’ or pol.
Genus SaccuutNeLya Crespin, 1958
Sacculinella australae Crespin
One specimen doubttully referable to this species was recovered from A.O.C.
North Renmark No. 1, 3,410-3,415 fect. Sacculinella Crespin has been synonyzn-
ized with Brachysiphon Chapman by Loeblich and Tappan, hut there seems to
be insufficient support for this view from the material available.
Genus ThuramMinomes Plummer, 1945
Thuramminoides sphaeroidalis Plummer
pl. 3, figs. 15, 16
1945. Thuramminoides sphaeroidalis Plummer, 218. pl. 15. figs. 4-10; Crespin, 1958. 49.
pl. 3. figs. 9-11; pl. 31, figs. 1-2; Conkin, 1961, 243, pl. 17, figs. 1-10; pl. 18. figs,
1-4; pl, 26, figs. 1-3.
Description. An amended description of the species. has been given by
Conkin (1961). South Australian specimens are always preserved as deHated or
flattened dises, The wall is finely arenaccous with agglutinated quartz grains
cemeénted by siliceous material in some tests and culeareous material in others.
Of 182 tesis examined 88 had calcareous cement; these all came from Stuart
Range No, 3 Bore with the exception of one specimen from Ware 5, locality
5/641/5, and three from Stansbury Stratigraphic Bore. The development of
protuberances on some of the tests is similar to that on Texas specimens,
Dimensions, The species shows a considerable range in diamcter as shown
by Conkin (1961, p, 247), with whose measurements (in mm.) those from the
different South Australian localities may be compared,
Locality 5/641/5 0-6 (1 specimen)
Stansbury Stratigraphic Bore )-4-0-5 (14 specimens)
Minlaton Stratigraphic Bore 0-4-0°7 (8 specimens )
Buorthanna Bore 4075 (10 specimens)
Lake Fhillipson Bore -25-0-63 (4 specimens )
Stuart Range No, 3 Bore Q-5-2-25 (69 specimens)
Nullarbor No. 8 Bore 0:5-1-0 (47 specimens)
The South Australian specimens are on the whole of medium size. The largest
specimens with diameter of 1-75 mm. or more are smooth specimens with pro-
tuberances (pl. 3, fig. 16).
Wall Siruciure. The problem of the cementing material and the possible
replacement by silica of original calcite is not resolyed in the present study.
PEHMIAN DEPOSITS GF S.A. AND FAUNA 77
Same tests of both Thuramminvides sphaeroidalis and Hyperammina hebdenensis
have calcareous cement in certain samples. Both species occurring in Ware
locality 5/641/5 and at depths of 1,225 to 1,367 feet in Stuart Range No. 3 bore
have both calcareous and siliceous tests in the same sample, Tests of Thuram-
minoides sphacroidalis have siliceous cement at depths of 740 to 1,225 feet and
calcareous cement below 1,367 feet in Stuart Range No. 3 Bore, while all the
tests in Minlaton, Boorthanna, Lake Phillipson, Stansbury, and Nullarbor No. 8
had siliceous cement. On the other hand, some tests of Hyperammina heb-
denensis from Nullarbor No, 8 have calcareous cement,
Australian Species of Vhuramminoides. Conkin_(1961, p, 243) has plaved
Crithionina tetcherti Parr, which was transferred by Crespin to Thuranminoides,
in synonymy with Thuramminoides sphaeroidalis. The two species are, in the
opinion of the present writer, specifically and generically distinct from each
other, Seven slides. containing some of Pars original type material were kindly
lent by the Department of Geology. University of Western Australia, While the
holotypes so far cannot be located slides 20768 and 20772 contain topotypes of
Crithionina teicherti from Part's original material, Slide 20765 has seven
mounted specimens which, with one exception 1-8 mm. in diameter, range from
2.0 to 2+5 mm. in diameter. They are spherical and uncrushed with a loosely
cemented wall 0-2 mmm. thick. The otherwise smooth outer surface of the wall
is marked irregularly by small openings of the irregular canals contained in
the thick wall. The inner surface is strongly and irregularly punctured with
larger openings.
From the limited amount of material available the genus Oryetoderma Loe-
blich and Tappan. 1961 (type species Crithionina rotundata Cushman) is to
be preferred for Crithionina teicherti. he test wall is relatively thinner than
illat of either the type species or of O. palacoxoica (Conkin), but the spongy
wull texture may be seen where there has been limonitic infilling, and the smal]
round or polygonal openings on the exterior surface are not characteristic of
Thuramminoides. The wall texture differs also from that of South Australian
specimens of Thuramminoides sphueroidalis, Oryctoderma teicherti has not se
far been recognized in the South Australian Permian.
Type Locality, Thuramaininoides sphaeroidalis was described trom the
Middle Pennsylvanian lower Strawn Shale, east of San Saba, Texas, U.S.A,
Material. Hypotypes GSSA Ff377, FfS78; 162 specimens.
Distribution. The species is widely distributed in Stansbury, Minlatun,
Boorthanna, Lake Phillipson, Stuart Range No. 3 and Nullarbor No. 4 Bores
and locality Ware 5 (5/641/5).
Stratigraphic Range, Middle Silurian te Permian.
Family AMMODISCIDAE
Subfamily AmMMODISCINAE
Genus Ammonpiscus Reuss, L862
Ammodiscus oonahensis Crespin
pl, 3, figs. 17, 18
1955. Ammorliscus conahensis Crespin, 69, pl. 12. figs. LO, TE,
Description, Test free, depressed in the centre, consisting of a small pro-
loeulus and lony undivided second chamber closely planispirally wound in ahout
6 yulutions with oecasional growth constrictions, sutures distinct, slightly de-
pressed; chamber in last volution broad; aperture at end of second chamber,
slightly arched.
78 NN, H. LUDBROOK
Dimensions, Hypotype, greatest diameter 0-825, thickness 0-20 mm.
Type locality. Oonah, Tasmania; Quamby Mudstone.
Material. Hypotypes GSSA Ff402, 403: 215 specimens.
Distribution. W.G. Goyder Donna No. 1, A.O.C, North Renmark No. 1,
Stansbury, Minlaton, Beach Petroleum Troubridge Shoal No. 1, Boorthanna,
Coorie Appa, Stuart Range No, 3 and Nullarbor No, 8 Bores: localities Balta 6
(5/640/6) and Ware 5 (5/641/5),
Stratigraphic Range. Lower Permian,
Genus Hemmiscus Schellwien, 1898
Hemidiscus balmei Ludbrovk sp. nov.
pl. 3, figs, 19-231
Description, Test fairly large, irregularly discoidal, depressed in the centre.
consisting of a proloculus and an undivided tubular second chamber at first
planispirally wound like Amunodiscus then coiling unevenly so that later whorls
lap over the earlier whorls on one side; there are about five volutions in a
specimen of diameter 2-4 mm.; growth constrictions may occur at the former
positions of the aperture; diameter of second chamber increasing very gradually;
aiken distinct. slightly depressed; aperture at the open end of the tubular
chamber.
Dimensions. Holotype F399 diameter 1-3 mm.; paratype F400 diameter
0-7 mm.; paratype Ff401 diameter 2-4 mm.
Type Locality. Stuart Range No. 3 Bore, 1.225 feet 3 ins.-1,246 feet depth.
Material. Holotype GSSA Ff399; paratypes GSSA FF400, 401; 212 speci-
mens, including 6] topotypes.
Distribution. Common in W.G, Goyder Donna No. 1 Well between 600 and
2,073 feet; Stansbury, Beach Petroleum ‘Tronbridge Shoal Na. 1, Boorthawna,
Coorie Appa, Stuart Range No. & and Nullarbor No, 8 Bores,
Stratigraphic Range. Lower Permian.
The specific name acknowledges the contribution made by Mr. B. E, Balme
to understanding the South Australian Permian.
Genus AMMOVERTELLINA Suleymanoy, 1959
Ammoyertellina(?) glomospiroides Ludbrook sp. nov,
pl, 3. figs. 22-26
1988. Ammetertella inclusa Crespin, 72, pl. 18, fig 5 (non Cushman and Waters).
Description. Test free, fairly small, consisting of a proloculus followed
without any distinct separation by an undivided tubular second chamber of
uniform diameter throughout; flatly streptospirally coiled in the initial stages
then more or less planispiral; in the final stages the tube swings over and em-
braces the earlier coils at Tight angles to its previous plane of coiling. Wall thick,
agglitmaling, consisting of quartz grains well cemented in siliceous cement:
aperture arched, at the end of the final coil.
Dimensions, Holotype greatest diameter 1-0 mm., diameter of chamber
0-25 mm.
Type Locality. Stuart Range No. 5 Bore, 1,265-1,285 feet.
Material. Wolotype GSSA F396, paratypes CSSA F397, 398; 230 specimens.
Distribution. Locality Ware 5 (5/641/5), Stansbury, Minlaton, Boorth-
anna, Lake Phillipson, Stuart Range No, 3 and Nullarbor No. 8 Bores.
PERMIAN DEPOSITS OF S.A. AND FAUNA 78
Stratigraphic Range. Lower Permian.
Observations. This is the species identified by Crespin with Ammovertella
inclusa (Cushman and Waters). Unlike A. inclusa the species is not attached
nor when sectioncd does it show the planispirally coiled early portion figured
by Conkin (1961, pl. 23, fig, 8) or the planispiral zig-zag type of coiling illus-
trated by Ireland (1956, text fig, 5, 6-14). The type of coiling differs from that
of Ammocertellina in that in the final stage the tubular chamber does not uncoil.
The mode of coiling, however, is irregular when compared with that of Glomo-
spira or Glomospirella. It appears to represent a style of coiling intermediate
between Glomospira and Ammocertellina. In many respects the species is close
to Clomospira articulosa Plummer, which coils in a haphazard, but compact,
fashion,
Genus GLtomospma Rzehak, 1885
Glomospira adhaerens Parr
pl, 4. figs. 1-4
1942. Glomospiru udhaerens Parr, p. 103, pl. 1, fig. 2; 1958, Crespin. 70, pl. 13, figs. 6. 7,
The South Australian specimens are attached to quartz grains, coiled in
Glomospira fashion, the wall is thick, with agglutinated quartz grains im a
siliceous matrix,
Dimensions. Hypotype F391 diameter 0-75, diameter of tube 0-15 mm,
near the end.
Type Locality. “Lingula beds”, south side of Minilya River, near Coolkilya
Pool, Wandagee Station; Quinnanie Shale.
Material. Hypotypes GSSA Ff391, Ff392, Ff£593; 64 specimens.
Distribution. Stuart Range No. 3 and Boorthanna Bores.
Stratigraphic Range. Lower Permian,
Genus GLomosrmeLLA Plummer, 1945
Glomospirella nyei Crespin
ph 4, fig. 15
1958, Glomospirelle nyet Crespin, 70, pl. 13, figs, 1-5,
Only the specimens from Lake Phillipson Bore are small and within the
range of the type series described by Crespin. There seems to be no criterion
but size to distinguish the specimens from Stuurt Range No. 3 Bore from G, nye,
Dimensions. Hypotype diameter 1 mm., diamctcr of tube 0-15 mm,
Type Locality. Cumdlego Crossing, Minilya River, Western Australia;
Cundlega Formation.
Material. Ilypotype GSSA F£394; 100 specimens.
Distribution. Locality Ware 5 (5/641/5), Lake Phillipson and Stuart
Range No. 3 Bores.
Stratigraphic Range. Lower Permian.
Subfamily ToLyPAMMININAE
Genus TouyrpamMMina Rhumbler, 1895
Tolypammina undulata Parr
pl, 4, figs. 6, 9
1942. Tolypammina undulata Parr, 104, pl. 2, fig, 2; 1958, Crespin, 72, pl. 19, figs. 7, 8.
The South Australian specimens are all small, about 0-5 mm. diameter
overall, commonly adherent to quartz grains or to tubes of Hyperammina
hebdenensis, as noted by Crespin.
&0 N. H. LUDBROOK
Type Locality. “Lingula beds”, south side of Minilya River, near Coolkilya
Pool, Wandagee Station, Western Australia; Quinnanie Shale.
Material, Hypotypes GSSA F{380, Ff381; 184 specimens.
Distribution. Locality Balta 6 (5/640/6), Stansbury, Minlaton, Boorthanna,
Stuart Range No, 3 and Nullarbor No. 8 Bores,
Stratigraphic Range, Lower Permian.
Genus AmMMOVERTELLA Cushman, 192
Ammoyertella howchini Ludbrook sp. nov.
pl. 4, figs. 6-8
Description. Test attached, consisting of a small proloculus followed by a
long narrow tubular second chamber which at first winds back and forth in 7ig.
zag fashion and later winds irregularly over the surface of attachment: wall agulu-
tinated with fine angular quartz grains in a small amount of siliceous ecment;
aperture at the open end of the tubular second chamber.
Dimensions, Holotype Ff414 diameter 1 mm. x 0-8 mm; hypotype Ff415
diameter 0-65 x 0-625; hypotype F416 diameter 0-9 x 0-8 mm. Size of the
tests is variable. The initial portion is usually about 0-5 mm, in diameter, but
the lotal area covered by a single specimen may be as much as 2 mm. or more;
diameter of tube 0-075 mm.
Type Locality. Cape Jervis; Cape Jervis Beds.
Material, The holotype Ff414, paratypes Ff415, 416, and 52 other specimens,
Distribution, Stuart Range No. 3 and Stansbury Bores: 2 pebble 36 mm. in
diameter from Stansbury Bore. is extensively covered with many encrusting
individuals.
Superfamily LrrvoLacea
Family HORMOSINIDAE
Subfamily [lonmosininaE
Genus Reorpwax Montford, 1908
Reophax subasper Parr
pl. 4, fiz. 15
1942. Reophax subasper Parr, 108, pl. 1, fig. 12; 1958, Crespin. 64, pl. 11, figs. 10, 11,
South Australian specimens have calcareous cement.
Dimensions. Hypotype length 0-8, width 0-4 mm.
Type Locality. “Lingula beds”, east of Coolkilya Paddock, Wandagee Sta-
tion, Quinnanic Shale.
Material, A single paratype on UWAGD slide 20770; hvpotvpe GSSA F389,
and 4 other specimens.
Distribution. Stansbury and Stuart Range No, 3 Bores.
Stratigraphic Range. Lower Permian,
Reophax (?) thomasi (Crespin)
pl. 4, figs, 16, 19. 20
1958. Lugtonia thomasi. Crespin. 65, pl, 7, figs. 6, 7.
Description. Test free, straight, flaring slightly, consisting of as many as
six chambers in a rectilinear series; sutures distinct, straight. depressed; wall ver
thick, agglutinating, with close set fine quartz grains in a small amount of cake
careous cement, leaving very reduced chamber cavities connected by necks;
aperture circular, terminal, surrounded by a thickened lip,
PERMIAN DEPOSITS OF S.A. AND FAUNA 81
Dimensions. Hypotype (incomplete) length 1-2, width 0-5 mm.
Type Locality. 14 miles southwest of Nalbia Dam, Wandagce Station,
Western Australia; Bulgadoo Shale.
Material. Wypotypes Ff389, Ff440; 30 specimens.
Distribution. A.O.C. North Renmark No. 1, Stansbury, Minlaton, Coorie
Appa, Stuart Range No, 3, Nullarbor No, 8 Bores.
Observations. Conkin (1961, p. 276) has discussed the anomalous position
of this reophacid species in the genus Lugtonia Cummings, which was placed
by its author in the Earlanditdac. Crespin (1958, p. 35) states that the Western
Australian specimens of R. thomasi have siliceous cement; South Australian
specimens have calcareous cement, In thin section no evidence can be seen of
the domed chamber form of Lugtonia, although most of the tests are poorly pre-
served and distorted. The thin section figured (pl. 2, fig. 20) shows the unustially
thick wall and reduced chamber cavity, while the nature of the initial part of the
test iy somewhat doubtful. For these reasons the geuus Reophax is used with
caution until sections can be made of a wider range of undistorted specimens,
Reophax tricameratus Parr
pl. 4, fig. 14
Five specimens, some complete, occur in Nullarbor No. § Bore, 1,280-1,290
feet. The species is large; the wall of South Australian specimens consists of
coarse quartz grains in calcareous cement,
Dimensions, Hypotype length 2, diameter 1-4 mm.
Type Locality. “Lingula beds”, south side of Minilya River, near Coolkilya
Pool, Wandagee Station, Western Australia; Quinnanie Shale.
Material. Paratype on UWAGD Slide 20772, hypotype CSSA FY390; five
specimens.
Distribution. Nullarbor No. 8 Bore, 1,280-1,290 feet.
Stratigraphic Range. Lower Permian ( Artinskian ).
Family LITUOLIDAE
Subfamily ITapLorpuRAGMOIDINAE
Genus Recurvomrs Harland, 1934
Recurvoides wilsoni Ludbrouk sp. noy.
pl. 5, figs. 1-10, 15
Description, Test free, subovate to flatly globose, asymmetrical, strepto-
spiral; first whorl is planispiral but later whorls in different planes; periphery
more or less oval, lobulate, chambers mumerons, about seven in the final whorl
increasing very gradually in size as added, inflated unless flattened during
fossilization, with pseudochitinous lining; sutures distinct, depressed, nearly
straight, wall coarsely arenaceous with coarse angular quartz grains in a siliceous
matrix; aperture interia-areal apparently a small low arch, with a lip.
Dimensions. Uolotype F403, greatest diameter 0-60, thickness 0-4 mm<¢
paratype Ff407, greatest diameter 1-25, thickness 1:0 mm.; paratypes are in
the range of greatest diameter 0-75-1-25 mm.
Type Locality. Cape Jervis, Cape Jervis Beds,
Muterial. The holotype Ff405, paratypes Ff406-F(413, Ff441; 348 speci-
mens.
52, NN. H. LUDBROOK
Distribution. Cape Jervis, Balta 6 (5/640/6); Stansbury, Minlaton, Beach
Petroleum Troubridge Shoal No, 1, Boorthanna, Stuart Range No. 3 Bores,
Observations. The genus Recurvoides has not previously been recorded
from rocks alder than Oligocene, The streptospiral test of Recurvoides wilsoni
is very variable in shape and when fully developed is most closely related to the
Recent R. turbinatus Brady, R. contortus Earland and &. trochamminiforme
Héglund, The avis of coiling in R. wilsoni as in B. trochamminiforme continues
to change throughout the development of the test. Immature specimens are
planispiral and similarly coiled to the genus Adercotryma,
Both &. contortus and R. trochamminiforme inhabit cold waters or fjords.
The relatively abundant numbers of B. wilsoni at Cape Jervis in beds deposited
in an over-deepened yalley or fjord appear to parallel the occurrence of R.
trochamminéforme in Gullmar Fjord. R. contortus occurs off South Georgia and
in Antarctic waters.
Species of bath Adercotryma glameratum (Brady) and Recurvoides turbi-
natus have been described from Arctic waters. Both species occur together at
several stations off Greenland, at depths of between 31 and 91 metres and also
off Humboldt Glacier at 201-2 metres (Loeblich and Tappin, 1953),
Sectioning of the test shows (pl. 5, fig. 15) the interior of the chambers to
be conspicuously lined with pseudochitinous material. FR, obsaletum (Goés) and
R, higeinsi Bronnimann from the Crise and Lengua Formations of Trinidad
have been described (Bronnimann, 1953, p. 98) as having the interior of the
chambers coated with a brown or thin ?chitinous film.
Specifie Name. The species is named for Mr. R. B. Wilson of Geosurveys
of Australia Ltd. who collaborated with the writer in selecting and describing
the type section of the Cape Jervis Beds,
Subfamily Lrrvotinar
Genus AmMopacutrrrs Cushman, 1910
Ammohaculites woolnoughi Crespin and Parr
pl, 4, fiz, 17
ID41. -Ammokaculites woolmwughi Crespin and Parr, 304, pl. 12, fius, 2a. Th. 3a, bh; 1958.
Crespin. 75, pl. 14, figs. 10, 11 (synonymy).
The three specimens from South Australia are poorly preserved and identi-
fication is doubtful. One specimen was recovered from Minlaton Bore, 554-560
fect, and one from Stuart Range No, 3 Bore at depths of 1,205 feet 5 ins. - 1,235
feet 5 ins. and 1,265-1,285 Feet,
Family TEXTULARIIDAE
Subfamily Trexrunagusar
Genus Textutania Défrance in de Blainyille, 1824
Textularia bookeri Crespin
pl. 4 fic, 18
141. Texbularia eximia Crespin and Parr, 305, pl, 13, figs, Tac. Su-c: 1947, Crespin, pl. 2,
figs. 23, 24 (non Bichwald).
1956, Textularia “exima Eichwald” of Orespin ard Parr, Cuuitnings, 214.
1058. Vertularia howkeri Crespiu, 77, pl, 15, fiys. 1-7.
South Australian specimens are usually distorted during fossilization and the
arrangement ot the carly chambers is difficult to determine.
Dimensions. Hypotype Ff383, length 1-1, width 0-$ mm.
PERMIAN DEPOSITS OF S.A, AND FAUNA a3
Type Locality. Four chains west of Farley Railway Station, Hunter River
District, New Sonth Wales; Dalwood Group.
Material. 40 specimens.
Distribution. Locality Ware 5 (5/641/5), Stansbury, Boorthanna and Stuart
Range No, 3 Bores.
Stratigraphic Range. Lower Permian.
Family ATAXOPHRAGMIIDAE
Subfamily GLOBOTEXTULARINAE
Genus Diertmxa Crespin and Parr, 1941
Digitina recurvata Crespin and Parr
pl. 4, figs. 10-12
1941, Digitina recurvata Crespin and Parr, 306, pl. 13, figs. 9a, b, 10a, b: 1958, Crespin, 79,
pl. 15, figs. 10, 11,
Description, Test free, moderately elongate, flaring, of moderate size, cou-
sisting of a minute trochospiral stage with about 4 chambers in the initial whorl,
followed by a triserial portion with about 9 inflated globular chambers increasing,
fairly rapidly in size, then becoming irregularly biserial and finally uniserial.
Sutures distinct, depressed; wall coarsely agglutinated with coarse angular quartz
grains in a thin matrix; aperture interio-areal, a very small arched slit near the
base of the apertural face. In the figured hypotype (F{418) and two other
specimens from Stuart Range No. 3 Bore, in which the uniserial stage has de-
veloped, the aperture is subterminal, as it appears to be in the holotype (Crespin
and Parr, pl. 13, figs, 9a-b).
Dimensions. South Australian specimens are relatively short and broad,
adult specimens from Stuart Range No, 3 Bore attaining a length of 1-0, width
0-7 mm; most Cape Jervis specimens come within the range length 0-4-0625,
width 0°325-0-45 mm,
Type Locality. Foot of Victoria Pass, Mitchell Highway; Capertee Group,
Material. 29 specimens.
Distribution. Cape Jervis, Stuart Range No, 3 Bore, 1,285-1,367 feet.
Observations. The genus Digitina has been retained here only because no
specimens of Mooreinella Cushman and Waters, 1928, are available for com-
parison. Cummings (1956, p. 214) suggested the possibility of the synonymy
of Digitina with Mooreinella which was rejected by Crespin (1958, p. 36) on the
basis of apertural differences. Although the aperture is usually, as Crespin
emphasizes, at the base of the final chamber, in fully adult specimens with a
uniserial final chamber, the aperture is, like that of Afooreinella, subterminal.
However, no description of Mooreinella mentions the triserial stage, through
which Digitina passes so conspicuously that the immature specimens from Cape
Jervis with poorly preserved initial portions appear to belong to Eggerella (pl.
4, figs. 11, 12).
Phylum MOULLLUSCA
Class GASTROPODA
Genus Peruviserra Chronic, 1949
The single minute inconiplete specimen 1 mm. diameter (pl. 5, fig, 13) is not
sufficiently well preserved for its specific identity to be established, but with its
veneric range of Lower to Middle Permian, it is an important element im the
fauna, The specimen was recovered from 1,285-1,805 feet in Stuart Range
No. 3 Bore.
&+ N. Tl. LUDBROOK
Gastropod indet. A minute stemkern of a protoconch also occurred in
Stuart Range No, 3 Bore at 1,327-1.349 fect.
Phylum COELENTERATA
Class SCYPITOZOA
Genus ? Coxunanta Sowerby, 1891
The fragment figured (pl. 5, fig. 14) of a pyritized cast appears ta be that
of a Conularia, from Stuart Range No. 3 Bore, 1,327-1,349 fect,
OTHER ORGANIC REMAINS
Two species of ostracodes (pl. 5, figs. 11, 12) were recovered from Stuart
Range No. 3 Bore, 1,327-1,349 feet, together with vertebrate teeth and bones.
ACKNOWLEDGMENTS
The writer is indebted to Professor R. T. Prider, University of Western
Australia, for the loan of the Parr slides, and to Miss Ruth Todd, of the United
Stafes National Museum, Washington D.C., and Dr. G. R. J. Terpstra of the
Bureau of Mineral Resources, Canbarss, for making comparative material avail
able during visits to their institutions, Dr. J. M. Dickins of the Bureau of
Mineral Resources, kindly supplied casts uf Peruvispira allundalensis. The
assistance of Mr. W. K. Harris and Miss L, D. Linke of the Palaeontology Section,
Geological Survey of South Australia, in photographing the specimens is grate-
fully acknowledged,
REFERENCES
Baume, B. E., 1957. Upper Palaeozoic microfloras in sediments from the Lake Phillipson
Rore, South Anstralia. Aust. J. Sei, 20 (2), pp. 61-62.
Bator, B. E.. 1964. The palynological tecord of Australian Pre-Tertiary floras. Ancient
Pacific Floras. Univ. Hawaii Press, pp. 49-80,
Broxyimann, P. 1953. Arenaecous Foraminifera from the Oligo-Miovene of Trinidad.
Contr, Cushinan. Fdn. foramin, Res, 4 (3), —pp. 87-L00.
Campana, B.. and Winson, BR. B.. 1953. The geology of the Jervis and Yankalilla Military
Sheets. Rep. Inyest. geol. Surv. S. Anst.. 3, pp. 1-26. pls. IX.
Campana, B.. and Wiisow, R, 8. 1985. Tillites and related glacial topography of South
Australia, Eclog, geol, Hely., 48 (1), pp. 1-30. pls. I-IV.
Canapte, J., and Sanity, L., 1965. The Pre-Mesovoic Geology of the Western Great Artestaiy
Basin, Australas. Petrol, Explor. Assoc. APEA J,, pp. [67-LL0.
Comman, J. E,, 1961. Mississippian smaller Peraminifera of Kentucky, southern Incliana.
northern Tennessee, and south-central Ohio, Bull. Amer, Paleant.. 43 (196), pp. 132-868,
Crespin, [, 1958. Pertnian Foraminifera of Australia. Bull. Bur. Miner. Resour. Ceal. Geo
phys. Aust., pp. 1-207.
Crespin, 1.. anche Park, W. J. 194). Arenaceous Foraminifera from the Permian rocks of
New South Wales. J. Proc. R, Soe. N.S.W,, LXXIV. pp. 300-311, pis. XIL-NTIT.
Cummanes, R. IT. 1956. Revision of Upper Palacozoic textulariid Foraminifera. Micro-
paleontology, 2 (3), pp. 201-242.
Damp, T. W. E., and Nowcurs, W., 1897. Notes on the glacial features of the Tnmun Valley,
Yankalilla and Cape Jervis District. ‘fYrans. R, Sov; 5, Aust, 21, pp, 61-67.
Preytac, LB. 1965. Mount Toondinu Beds — Permian sediments in u probable: piercement
structure. Trans. R, Soc. $, Aust.. 89, pp. 61-76, pls, L-LIT. ;
CGnren, W. J., 1965. The Gidgealpa Cas Field. Australas, Petrol. Explor. Assoc. APEA J.
1p, G5-GH,
Hanns, W._K.. amd Lupssoox. N. H., 1966, Occurrence of Permian sediments in the Fuela
Basin. South Australia. Quart. veol, Notes, geol, Surv. S. Aust., 17. pp. 11-14.
Thi, D., 1955. Contributions to the correlation and fyuia of the Permian ir Australia and
New Zealand. J. geal, Soc. Aust, 2. pp. 84-107. ;
Howes, W.. 1895. New facts bearing on the glacial features of Hallett’s Cove. ‘Trans.
R, Sov. $, Aust, XIX. pp. 61-69.
PERMIAN DEPOSITS OF S.A, AND FAUNA $3
Howcmx, W., 1910. The glacial_(Permo-Carbonifcrous) moraines of Rosetta Head and
King’s Point. South Australia, Trans. R. Soc. S, Aust., XXXIV, pp. 1-12. pls, L-XVU.
Hower, W., 1926, The Geology of Victor Harbour, Inman Valley and Yankalilla Districts
with special reference to the great Inman Valley glacier of Permo-Carboniferous age.
Trans, R. Soc. 8. Aust., L, pp. 89-119.
Inccanp, H. A,, 1956. Upper Pennsylyanian arenaceous Foraminifera from Kansas. J.
Paleont, 80 (4), pp. 831-864.
Kaper, A., 1966, The Cooper's Creek Basin, Australas. Oil Gas J., 12 (9), pp. 24-30,
Lorpiics, A. R,. and Tappan, IL, 1953. Studies of Arctic Foraminifera, Smithson. Misc.
Coll, 121 (7), pp. 1-150.
Lorsuicu, A. R., and Tappan, H., 1964, Protista 2. Part C, Treatise on Invertebrate
Paleontology. Geol. Soc, Amer. and Kansas Univ, Press.
Luvunoox, N, H.. 1956, Permian Foraminifera in South Australia, Aust. J, Soi. 19 (4).
pp. 161-162,
LuparooK, N. H., 1961. Permian to Cretaceous subsurface stratigraphy between T,ake Phil-
lipson and the Peake and Denison Ranges, Trans, K. Soc, 5. Aust., 85, pp. 67-80,
Lupproox, N. H., 1966a,_ Minlaton and Stansbury stratigraphic bores. Appendix to Craw-
fare, A. R,. The Geology of Yorke Peninsula. Bull. geol, Surv, S. Aust., 39, pp, 83-96,
g. 1.
Luynnoox, N. H., 1966b. Cretaceous biostratiyraphy of the Great Artesian Basin in South
Australia. Bull, geol, Surv. $8. Aust., 40, pp. 1-223, pls. 1-28, figs, 1-34, maps 1-11.
Lunprook, N. H., 1967, Stuart Runge No. 8 Bore, Cooher Pedy: Stratigraphy and Micro-
palaeontology, Min, Rey. Adelaide, 122 (in press).
Mawson, D., 1926, Varve shales associated with Permo-Carhonifcrous glacial strata of South
Australia, ‘Irans, R. Soc, S, Aust., 50, pp. 160-162,
Moorcrort, E,. 1964. Geophysical Investigation, Mt. Toondina Area. Quart. geol. Notes,
geol. Surv. S. Aust., 12, pp. 4-6.
Parr, W. J,, 1942. Foraminifera and a tubicolous worm from the Permian of the North-west
Division of Western Australia. J. R. Soc, W. Aust.. XXVIL, pp. 97-115.
Poumsen, H. J., 1945. Smaller Foraminifera in the Marble Falls, Smithwick and Lower
Strawn Strata around the Llano Uplift in Texas. Uniy. Texas Public:, 4401, pp. 209-271.
Reyxer, M. L.. 1955. The geology of the Peake and Denison Region, Rep, Invest. geol.
Surv. S, Aust., 6, pp. 1-23, pls, J-TV.
Spruce, KR. C., 1966, Palaeogeography of the Australian Permian in relation to oil search,
Australas. Petrol. Explor. Assoc, APEA J., pp. 17-29,
Worrner, H., 1964, Permian-Jurassic history of the western Great Artesian Basin. Trans.
R. Soc. S. Aust., 88, pp, 117-128.
Worrner, H., 1966. CGidgealpa Gas Field, South Australia. A case history. Australas. Oil
Gas J., 12 (11), pp. 29-53.
Figs.
Fig.
Figs.
Fig,
Figs,
Fig.
Figs.
Figs.
Figs.
Figs.
Figs.
Figs.
Figs.
bo
gah ne
4,
1-4.
5, 9.
6-8,
N. H, LUDRROOK
EXPLANATION OF PLATES
Prate 1
Cape Jervis Beds (C.J.) overlying Kanmantoo greywacke (K) at south end af
type section, View southerly.
View upwards through units 2 and 3 of Cape Jervis Buds to sandstone ledge of
viait 4, showing inter-bedded sandstone and clay of anit 2. and boulders in
ayers.
Southerly view of same part of section a4 Fig. 2, showing dip in lower part of
section and bedding of boulders,
Striated houlder on tillitie clay at northern end of type section,
Prate 2
Gully erosion in Cape Jervis Beds, north end of type section,
Erratic in boulder clay overlying Selwyn’s rock (lower left), Inman River,
King’s Point, Encounter Bay: boulders on shore at foot of point overlain by
boulder till, with sandstone at top right.
Burrowings in sandstone at t6p of section, King’s Point, This part of the sequence
is doubtlully of Permian age.
Pirate 3
All Figures X 30
Hippocrepinella biaperta Crespin, F379, Minlaton 500-530 feet:
Hyperammina hebdenensis Crespin, 2, F13T4a, with siliceous cement: 3, FF374h,
with calcareous cement, both locality 5/641/5; 4. Ff373. with siliceous cement,
Stansbury 845 feet; 5, F375, with calearcous cement, Nullarbor No. & 1290-
1300; 6, M376, with siliceons cement, North Renmark No, L 3755-3760 feet.
Hyperammina acicula (Parr), £370, Stuart Range No, 3, 1205.5-1295.5 fect,
Hyperammina coleyi Parr. F{371a: b, Cape Jervis CT8. ;
Hyperammina expansa Plummer. Ft372, North Renmark No. 1, 3785-3790 feet.
Saccamminu orca Imdbrook, 11. holotype Ff384; 12, F386, paratype both
from Stuart Range No. 3, 1505 feet 8 ins, -1327 feet; 13, paratype F385, Stuurt
Range No. 3, 1827-1349 fect.
Fepenavtirtis ampulla (Crespin). F£387, Stuart Range No. 3. 1305 feet 8 ins. -
1827 feet.
Thuramminoides spheeraidalixy Plummer, 15, F377, with siliceous cement,
Stansbury 830 feet; 16, Ff378, with calcareous cement, Stuart Range No. 3,
1305. feet & ins. - 1327 feet,
Ammodiseus oondhensis Crespin. 17, F402, North Renmark No. 1, 3900-3905
feet: 18, FI403, Stuart Range No, 8, 1020-1040 feet,
Hemidiscus halmei Vudbrook, 19, holotype. FF399, Stuart Range No, 3. 1225
feet G ins.- 1246 feet; 20, paratype, FHO00, Nullarbor No. 8, 1320-1333 feet:
21. Ff401, Donna No. 1, 870-880 feet.
Ammutvertellina glomaspiroides Ludbrook, 232, holotype, FI396, Stuart Range
No. 3, 1265-1285 feet, the aperture eun be scen at the top of the Figure; 23.
holotype, reverse side; 24. paratype, Ff397. Stansbury, 210-215 feet. 25. 26,
two views of paratype F£398, Stansbury, 775 feet.
Puiare 4
All Figures X 30
Glomospira adhaerens Parr, 1, 2, two views of Ff89T. Stuart Runge No, 3,
1225-1246 feet, the quartz grain to which the specimen is adhering occupies
the central half of Fig. 2; 3, F£393, Stnart Runye No. 3. 1182-1205.5 feat:
4, Ff393, Stuart Range No, 3, 1367-1400 feet. wound around quartz grain.
Tolypammina undulata Parr. 5, F381, Minlaton, 500-530 fect. a 1ering to
Ryperammina hebdenensis; 9, FE380, Stansbury, 775 fect, adhering to «qnartz
grain,
Ammovertella howchini Ludbrook. 6, holotype. F#414, Cape Jervis; 7. para-
type, Ff415, Cape Jervis, showing aperture at the end of the tube on the right-
hand side of the Figure: 8. paratype, Hf416, Stuart Range Ko, 3, 1020-1040 feet.
Figs.
Figs.
Fig.
Fig.
10-12.
13.
14,
15.
16, 19,
Le.
18,
PERMIAN DEPOSITS OF S.A. AND FAUNA 87
Digitina recurvata Crespin and Parr. _ 10, Ff418, Stuart Range No. 3, 1305 feet
8 ins - 1327 feet; 11, 12, Ff417a, b, Cape Jervis.
Glomospirella nyei Crespin. F£394, Stuart Range No. 3, 1265-1285 feet.
Reophax tricameratus Parr. F£390, Nullarbor No. 8, 1280-1290 feet.
Reophax subasper Parr. F388, Stuart Range No. 3, 1349-1367 feet,
20. Reophax thomasi (Crespin). 16, 19, Ff£389a, b, Stuart Range No. 3, 1040-
1060 feet; 20, Ff440, thin section, North Renmark No. 1, 3785-3790 feet.
Ammobaculites woolnoughi Crespin and Parr. F£395, Stuart Range No. 3,
1265-1285 feet.
Textularia bookeri Crespin, F£383, Stuart Range No. 3, 1060-1120 feet,
PLATE 5
All Figures X 30
1-10, 15. Recurvoides wilsoni Ludbrook. 1, holotype, Ff405, Cape Jervis; 2, paratype,
11, 12.
13.
14.
Ff407, Stuart Range No. 3, 1182-1205.5 feet, spiral view; 4, Ff407. apertural
view, showing large quartz grain on apertural face; 4, Ff409; 7, Ff412; 9,
Ff410: 10, Ff411, showing change in plane of coiling; 5, if406, showing
apertural lip; 6, Ff408; 8, Ff413_ showing position of aperture; 15, Ff441,
Stuart Range No. 3, 1205.5 - 1225.5 feet, thin section, showing pseudochitinous
lining of early chambers.
Ostracodes, Stuart Range No, 3, 1327-1349 feet.
Peruvispira sp., M3180, Stuart Range No, 3, 1285-1305 feet.
? Conularia sp. Cr.3, Stuart Range No, 3, 1327-1349 feet,
PLatrr |
LupBRooK
H.
N.
3
o
4
FH.
N.
N. H. Luprroox
a
Puare 3
N. H. Lupsroox PLate 4
N. H. Lupsrook PLATE 5
FORAMINIFERA AND STRATIGRAPHY OF THE TYPE SECTION OF
PORT WILLUNGA BEDS, ALDINGA BAY, SOUTH AUSTRALIA*
BY J. M. LINDSAY}
Summary
The type section 20 miles (32 km) south of Adelaide has been reexamined. Comprising about 107
feet ( 32'/ m.) of bryozoal calcarenitic impure limestones, sands, silts, and clays, it is informally
subdivided into three apparently conformable successions of beds, the middle interval characterized
by horizons with spicular cherty nodules. Equivalents of these three intervals are present in the
Willunga Bore W.B.1, and in bores in the Adelaide Plains Sub basin. The top of the
Eocene Aldingan Stage is represented by the top of a hard grey marker bed at the base of the
siliceous interval about 45 feet (14 m.) above the base of the formation.
Planktonic and benthonic foraminifera indicate that the age of the section ranges from
Upper Eocene to Oligocene. Four informal planktonic zones are recognized, using successive
extinctions of Turborotalia aculeata (Jenkins), Globigerina linaperta (Finlay), Chiloguembelina
cubensis (Palmer) and Guembelitria stavensis Bandy. These zones span Aldingan to lower
Janjukian Stages, and can be related to a planktonic zonal scheme recently proposed for
New Zealand,
FORAMINIFERA AND STRATIGRAPHY OF THE TYPE SECTION OF
PORT WILLUNGA BEDS, ALDINGA BAY, SOUTH AUSTRALIA*
by J. M. Linpsart
[Read 13 July 1967]
SUMMARY
The type section 20 miles {a2 km.) south of Adelaide bas been re-
examined, Comprising about 107 feet (32% m.) of bryozoal calearenitic impure
limestones, sands, silts, and clays, it is informally subdivided into three. ap-
parently conformable successions. of beds, the middle interval characterized by
horizons with spicular cherty nodules. Eqnivalents of these three intervals are
present in the Willimga Bore W.B.L, aud in bores. in the Adelaide Plains Sub-
basin, The top of the Eocene Aldingan Stave is represented by the top of a
hard grey marker bed at the base of the siliceous interval about 45 feet (14 m.)
above the base of the formation,
Planktonic and benthonic foraminifera indicate that the age of the section
ranges from Upper Eocene to Oligocene. Four informal planktonic zones are
recognized, using snecessive extinctions of Turborotalia aculeata (Jenkins),
Globierine linaperta (Finlay), Chiloguembelina cubensiy (Palnier) and
Guembelitria stavensis Bandy.” These zones span Aldingan to lower Janjukian
Stages, and can be related to a planktonic zonal scheme recently proposed for
New Zealand.
INTRODUCTION
Rocks referred to Port Willunga Beds comprise a significant part of the
Tertiary sequence in the St, Vincent Basin and its sub-basins. Investigation
of the type exposure of Port Willunga Beds has therefore been a uecessary step
towards an understanding of the place of the formation in sequences elsewhere,
especially in the Adelaide Plains Sub-basin.
The type séction of the formation at Aldinga Bay, 20 miles (32 km,) south
of Adelaide (Fig. 1), forms part of the coastal exposure of the Cainozoic rocks
in the Willunga Sub-hasin of the St. Vincent Basin. Following interest in the
sequence over a period of at least 75 years by geologists and palaeontologists,
it was mapped, described, and formally subdivided and named by Reynolds
(1953). The Port Willunga Beds consist of a bryozoal calcarenitic series of
variable hard and soft rocks including impure limestones, sands, silts, and clays,
with an interval characterized by horizons of siliceous nodules, The beds,
which are well exposed in low coastal cliffs around the central part of Aldinga
Bav, have gentle southerly dips of up to 3° but are in part slightly folded and
faulted (see Fig. 2). They are now estimated to be about 107 feet (32% in.)
thick which is close to Reynolds's figure. Following Ludbrook (1936, p. 17), the
basal bed is taken to be the thin gravelly sand (sample 119-66 of the present
series) which overlies with minor disconformity the green fossiliferous clay
* Published with the permission of the Director of Mines.
} Palaeontologist, Geological Survey of South Australia.
Trans, Roy, Soc. S. Aust. (1967), Vol. 91.
4 J. M. LINDSAY
é - 7
as the top unit of Clinaman’s Gully Beds, The Port Willunga Beds are overlain
by Pliscene Hallett Cove Sandstone with mild angular unconformity,
bed (118-66) included by Reynolds in Port Wilhinga Beds, but now regarded
REFERENCE
Tor Walury Beds oyterap,
Sevenpe riwtetims.
Prams
WIiKL LONG A
Port Hoarlungs,
s FINE
Te tthe ey
4=n
Fig. 1, Locality map and plan showing position of samples taken from stratotype Port
Willunga Beds.
METHODS
Fig. 1 shows the localities at which samples were taken and Fig. 2 their
stratigraphic positions. Included are samples. from a pit dug at the site of
129-66, and also tube samples from a “Wacker” hammer hole sunk from the
bottom of the pit until stopped in hard sandstone, Washed and unwashed
samples and microfaunal preparations, are held in the Palaeontology Section of
the Geological Survey of South Australia.
The photographs of planktonic foraminifera in Plate 1 were taken with a
Leitz Laborlux microscope, using a Leitz Ultropak lighting unit in combination
with a 6.5X objective and relicf condenser, Adox KB 12 film was used, and
prints were made on Agfa Brovera paper.
CORRELATION ACROSS ALDINGA CREEK
The exposed Port Willunga Beds are divided into a northern and a southern
portion by the sand-covered and alluvium-filled entrance to Aldinga Creek, as
shown in Fig. 1, In order to consider the sequence as a whole, it is thercfore
necessary to determine the stratigraphic relationship between the northern and
southern sections across the distance of more than 800 feet (244 m.) which
separates them, There are several reasons why this is not a simple matter,
Firstly, some of the beds are observed to vary IJaterally in thickness and litho-
logy. As early as 1878, Tate noted their “most diversified character — clays,
limestones, and sands rapidly replacing one another in horizontal and vertical
95
A BEDS
'
4
c
FORAMINIFERA AND STRATICRAPHY OF PT. WILLUN
aWws
SIWLIW Oz i)
HO0d 4 aN 2 3 0 Did (| ANADOZ 4Yadadn
J5y15 NVTVELSNY NYIMOPNY CE NvyoONIOdYV
ES
= al.
JNOZ DINOLINWd — eraiagwenc! srseaqna EUSA BWD Bydadeny elildaiigeyg HIPSHIZE BYPIOJOQUAL
fe oi >
v
7
f
c
TEST RAeYS i é ue ._— te
SBuBGR? BU 7 Sn rh
Piswayzmanbinw 42 oF
nS
'
"
”
”
(3-5
Frequent (6-10
PanLigaeng 1) Le
SOARES Buk Wedio “Dp Waist:
Very rara (! - 2 specimel
Rare
Common {1-25
Abundant (25+
wa
SINRREOTEEWIN RUN NCEE)
Beneaesxenraed SeAPV Ng
aaaNNN JTdW¥S
TWAWSINI TidWvS | i :
WaaH9 YSNICIY 40 Hk va 5 tf
ALNOS ASOTOHLIT ; AU deat pai Sood LAO stl
VEG Shi
PCH] WILLUNGA BEDS
CHINAMANS GULLY BEDS’
@ SF 1NGON ALYSHD WLM TAU SIN I “Wea WONIOTW 40
NOILOSS DILYWAVHSVId GaAgANNS La Hen AAI
WAI VONIAIY ssoedov TWAYAIN| TAN ys
SQ3q VWONNITIM 1HOd 320 NOILOAS 3dAL 30 NO|LYTayYdOD dalsa5ens WRWNK Id WHS
dD aS Od) STH13N
SetAMOT A? TALI
Sessa? Pls vet Cad THT
waeut sisdevelngar)
Sua rhaysa ka
PLEA Beep hdagurs Se ae ID TM meet
eadeul t) | ee OE Se
— SS > Se
| a fh a
—
ee—_——
——
o——Sal > >
Pe tO
Sees tee
——$>> er
Foraminiferal log, lithology, and stratigraphy of stratotype Port Willunga Beds.
Fig, 2.
Hil J. M. LINDSAY
sequence as shown in Fig. 2. It is likely that the concealed section has beon
affected by one or more of these factors,” In addition, matching of the sections
immediately north and south of Aldinga Creek is rendered more diffieult by the
limited thicknesses available for examination.
Glaessner (1951, p, 275), recording the measurement by Dolling in 1949
ot 25 feet (74 m.) of “polyzoal sands and clays” north of Aldinga Creek, and
87 feet (30 m.) of “polyzoal sandy marls” south of it, listed these thicknesses
as consecutive and did not discuss the relationship between the two sections,
Reynulds did not explicitly state the thickness of beds common to both exposed
sections. Tn his Fig. 1, this thickness is apparently drawn as nine feet (2-7 m.).
In his more detailed and definitive Fig, 2 it is shown to be little more than two
feet (0'6 m.), However, in both of these representations the total thickness of
the formation is 111% fect (34 m.). Glaessner and Wade (1958) produced
from these data a composite section with the same total thickness.
At the time that Ludhrook and Lindsay (1966) recorded their preliminary
notes.on the range of Globigerina linaperta and the extent of the Aldingan Stage
within the formation, the writer accepted Reynolds's correlation of beds either
side of Aldinga Creek as shown in his Fix, 2.’ However, the ranges of Turboro-
tulie aeuleata in the northern and southern sections suggested that more of the
heds than he indicated in Fig, 2 are common to the two sections.
Later in 1966, during 2 discussion with Mr, W. Stewart of the Geology
Department, University of Adelaide, it became apparent that further measurc-
iments should be made to check the thickness common to both sections. In a
brief stadia survey, several marker beds near Aldinga Creek were traced by
the writer, and the results are presented slightly diagrammatically in Fig, 2.
The green clay with white limy nodules, which was used as‘a marker bed by
Reynolds and from which his sample 4.21) and the writer's sample 182-66 vere
taken, is matched with one of the green clays north of the creek as shown.
Both beds contain the uppermost occurrence of Turborotalia aculeata in their
respective sections, This correlation is considered to be reasonably consistent
with the lithological, structural, and microfauna] data, but it is certainly desir-
able that the depth to Chinaman’s Cully Beds should he proved south of Aldinga
Creek hy drilling.
The type section of Port Willunga Beds as now re-measured, is therefore
approximately 26 feet (8 m.) thick north of Aldinga Creek, and 89 feet (27 m_)
thick south of it, with nearly 8 feet (24 m.) of overlap between the secticms,
yielding a total thickness of about 107 feet (324 m.).
extension” Secondly, minor fulding and faulting sre apparent in parts of the
LITITOLOGICAL. UNITS
Reynolds, in his Fig. 2, distinguished 29 lithological units in the type section,
His basal bed, a green fossiliferous clay, is now considered to he the top unit
of Chinaman’s Gnily Beds, The remaining 28. units may be grouped into three
lithological subdivisions which are recognizable elsewhere in the Willunga and
Adelaide Plains Sub-basins. For the present, these three subdivisions ate simply
referred to as the lower, middle, and upper sequences, but [ture work may
show that they merit formal stratigraphic status.
Numbering Heynolds’s 28 units from the bottom up, the lawer sequence
contains units | to 12 and is by present measurement aud correlation about 43
FORAMINIFERA AND STRATIGRAPHY OF PT. WLLLUNGA BEDS a7
fect (13 m.) thick. It consists of a thin basal gravelly sand fallowed by
cream cross-bedded bryozoal calearenitic sandy limestones, calcareous sand-
stunes and sands, green-grey clays (often with white limy nodules) and fawn,
brown, or pale grey, impure calcarenitic limestones, silts and marls, Tris
variable succession extends up to the base of the first hard bed which has some
silicvous vernentation — the “hard consolidated grey marly bed ta be seen in the
caves below Port Willunga” (Reynolds, Fig. 2),
The middle sequence consists of most of the remainder of the type section,
up to and including the lowee part of unit 26. It is ahout 52 fect (16 m.) thick,
und is characterized by the sporadic development of a hard spicular cherty
phase typically oecurring as hands of fawn and grey fossiliferous cherty nodules
in saftey [awn-te pale grey impore limestones, silts, and mmarls, all calearenitic
and sandy, At the base of this interval is the hard marker bed noted above,
which has same siliccous phase but ix mostly limestone to caleareous siltstone
and sandstune. The base of the lowest bed with prominent siliceous nodules
is from 4 ta 5 feet (1-3 ta 1-5 m.) above the top of the marker bed. ‘This
middle, silievous, wterval in Port Willunga Beds is distinct from the alder
siliceous beds developed in Rlanele Point Banded Marls, The two are separated
by about 107 feet (32% m.) of Blanche Point Soft Marls, Chinaman’s Gully Beds
and Aldingan Fort Willunga Beds in the exposures at Maslin and Aldinga Bays.
The npper sequence comprises the upper part of unit 28 to the top ot the
exposed seetion, [t is about 12 feet (34 m-} thick, consisting, of yellow-brown,
fawn, and pale grey byrozoal beds including hard limestone bands, softer imoure
himiestavies. silty sands, and at the top of the exposure cross-bedded calcarenitic
Siinclstomes.
Reynolds did not define the top of Port Willunga Beds bul simply nnted
that the top of the formation is not reyealed in the type section. ‘Three and a
half miles (5% kro.) inland, the Wilhinga Bore W.B.L. (Clacssner and Woudard,
1958: Ludbrouk, 1956; Lindsay, 1966) penetrated, above the stratigraphic level
of the top of the type section, more than 160 fect (49 m,) of calcareans sands,
sandstones, and santly limestones, which are evidently also Port Willunga Heds.
They extend up beyond the level of Janjukian (Oligocene) beds at the top of
the type section inte beds which are Longfordiun (Lower Miocene). Thr three
lithological subdivisions of the type section can also he recognized in broad
outline in the bore, despite changes there in lithotacies due to depesition under
more marginal and restricted couditions.
Calearenitic limestones, sands, and clay, which may be included within the
scope of Port Willunga Beds, ure widespread in the St. Vincent Basin (Glaessner
and Wade, 1958). Im the Adelaide Plains Sub-basin Miocene beds up to Bal-
combian Stage, including the Manno Para Clay Member, are known trom bores
(Lindsay and Shepherd, 1966), and in one locality the presence of Heterolepa
victoriensis (Chapman, Parr and Collins) suggests Bairnsdalian Stave (Lindsay,
19635), It has been recently demonstrated (Lindsay. 1967) that equivalents nf
the three lithological subdivisions of the type section are recognizable in deeper
bores in the Adelaide Plains, The middle, siliccous, interval is well-developed
al least as far north as Hundred of Dublin, but the lower interval is ditheult to
separate from Blanche Point Soft Marls, and Chinaman’s Gully Beds usually
camot be distinguished. The whole succession of Port Willingu Beds attains
a maximum known thickness of 874 fect (267 m.) in the Croydon Bore, where,
in the lower part of this succession, equivalents of the type section are 440 feet
(125 m,) thick,
Oe ]. M. 1A4NDSAY
CORRELATION WITH AUSTRALIAN AND NEW ZEALAND STAGES
After tracing the usage of the stage name Aldingan, Ludbrook and Lindsay
redefined the term “in the restricted time-rock sense as representing the time
iuterval required for the deposition at Aldinga and Maslin Bays of the Torta-
chilla Limestone, the Blanche Point Marls, the Chinaman’s Gully Beds, and the
Jower half of the Port Willunga Beds*. The upper boundary of the stage was
drawn at a level of natural subdivision, invelving both an important micru-
faunal event — the top of the range of Globigerina Tinaperta —and an important
lithological development — the commencement of the middle, siliceous, interval
of Port Willunga Beds, The end of the Aldingan Stage is now further defined
as heing represented by the top of the hard grey marker bed which is the basal
unit of the middle interyal as described above. By prescut measurement and
correlation the boundary is at approximately 45 feet (14 m.) above the base of
the formation.
Raggatt and Crespin (1955), followed more recently by Carter (1964),
have restricted the Janjukian Stage in a time-rock sense to xepresent the time
interval required for the deposition of the Jan Jue Formation in the Bell's Head-
land-Torquay area of southern Victoria, The most diagnostic planktunic event
at present available to link the type sections of Jan Jue Formation and Port
Willunga Beds, is the extinction of Chiloguembelina cubensis which takes place
near the base of the former aud near the top of the latter, This event is a feature
of Carter's Faunal Unit 4, in the lower episode of the Janjukian. Prom available
data on the range of the species’ in both sequences it may be inferred that Jess
than 20 feet (6 m.) of Port Willunga Beds, at the top of their type section, are
early Janjukian. Most of the middle, siliceous, interval appears to be strictly
pre-Janjukian and it is post-Aldingan us at present defined. Further description
of the Jan Juc Formation and its planktonic foraminifera will be necessary to
further clarify the relation between Aldingan and Janjukian Stages.
Comparison of the ranges of several planktonic species in Port Willungs
Beds with their ranges as recorded by Jenkins for New Zealand, suggests cor-
relation with the Kajatan, Runangan, and Whainguroan Stages as shown in
Fig. 2.
AGE OF THE TYPE SECTION
Eucene age was recently uscribed to the lower, Aldingan, part of the type
section by Ludbrook and Lindsay, the writer having recognized in it a foramini-
feral succession, apparently unaffected by reworking, containing Clobigerina
imaperta and associated Eocene species. Although in carlicr years considered
all of Eocene age by Tate (1879, 1899) and ‘late and Dennant (1896), the type
section was more recently considered to be of Oligovene to Lower Mincene age.
Tlw foraminiferal evidence now available suggests an Oligocene age for the
post-Aldingan part of the section,
PLANKTONIC ZONES
Lithologics and microfannus suggest that stratotype Port Willunga Beds, as
indeed most of the marine ‘Tertiary of the St. Vincent Basin, were deposited
under conditions of somewhat restricted access from the open ocean, This eu-
vironment does not favour the presence of the tropical or temperate planktonic
foraminifera which have been chosen to diagnose planktonic zones in standard
sequences of comparable age elsewhere. For cxample, of the zonal species of
FORAMINIFERA AND STRATIGRAPITY OF PT, WILLUNGA BEDS 99
Blow and Banner (1962), only Globigerina ampliapertura Bolli has been found,
Zonal species of Jenkins (1965) not yet enconntered_ inchide Glohoratalia in-
conspicua Howe, and Clobigerina brevis Jenkins. Globigerapsis index index
(Finlay), key species of the index zone or zouc 2 of Carter (1964, p. 46) fol-
lowed by Wade (1964), occurs only very rarcly and as immature specimens.
Globigerina angiporoides angiporoides Hornibrook, another of Jenkins’s zonal
specics, althmgh very rare, is typical and persistent within the range of G.
Linaperta s.str. Above this, however, only occasional doubtful specimens are
preserit at the level of the angéporoides angipervides zone in New Zealand, and
the zone is thus not suitable for local use. G.-evapertura Jenkins is present,
but not well-developed in the type section, Jenkins, however, defined the lower
boundary of his evapertura zone by the extinction of G. angiporoides angi-
puroides, and as noted above this is nat a suitable criterion at Aldinga Bay.
The linaperta zone of Carter (1964) followed by Wade 1964), was equated
by them with Carter’s Faunal Unit 8, which is characterized by the microfauna
ol the upper part of the Castle Cove Limestone, and the “Lower Glen Aire
Clays”, containing “a form of Globigerina linaperta with swollen chambers”
(Carter, 1958, p. 21). Examination of available material leaves little doubt that
this is C. angiporoides ungiporoides, and not G. linaperta s.str, Jenkins records
similar upward ranges for both G. linaperta and Globigerapsis index index in
New Zealand. Faunal Unit 3, or the “linaperta zone” in this sense, has not been
used in the present study due ta some uncertainty as to the planktonic content
and sttatigraphic position of the beds used to define it.
Jenkins defined a different zone of C. linaperta in the Upper Eocene of
New Zealand, between the extinction of Globorolalia inconspicua and the initial
appearance of Globigerina brevis, Neither of these species is known from Port
Willunga Beds but his zone is adapted for local use as described below-
The most useful characteristic of Carter's Faunal Unit 4, the final appear-
ance of Chilozuembelina cubensis, is utilized as the upper limit of a zane of C,
cubensis which follaws the zone uf G, Iinaperta, Guenrbelitria stavensis is asso-
ciated with C. cubensis at the level of Faungl Unit 4 and ranges a little higher.
This relationship is used to define a zone of GC. stavensis, which occurs at the
top of the type section.
Despite their usefulness at a certain stage in the development of Australian
Tertiary stratigraphy, Carter's Faunal Units or Zones are for various reasons
proving unsuitable or difficult to use (at least in the Eovene and Oligocene)
as a framework for planktonic zonation. The recent work of Jenkins im New
Zealand has provided the basis for an alternative approach and it is therefore
proposed to define from stratotype Port Willunga Beds, informal local plank-
tonic zones which may be nseful within the St. Vincent Busi, and may also
be velated to zones elsewhere via more diverse planktonic sequences from
southern Australiz and New Zealand,
The Jowest such zone in the type section is that of Turborotalia_aculeata
(= Globorotalia inconspicue aculeata Jenkins) which extends below Purt Wil-
tunga Beds, and whose upper limit is marked hy the top of the range of the
species, Jenkins ceenrded the same extinction level for h of the forms he
regarded as subspecies of G. inconspicua. if 7. aculeata has a similar range
in South Australia, the basal 22 feet (6-7 m.) of Port Willunga Beds containing
the species, correlate with part of ihe Kaiatan Stage of New Zealand at the
top of the zone of G. inconspicua. Species associated with 1’. aculeata in the
aculeata zone at Aklinga Bay include Globigerapsis index tudex, Globigerina
100 J. M, LINDSAY
lineperta, G. angiporovides angiporoides, G. anpliapertura, Turkorotalia incre-
beseens { Bandy), Chiloguernbelina cubensis, and Cassiverinella sp. cf. C. chipe-
lensts (Cushman and Ponton). Below Port Willunga Beds, the sequerice at
Aldinga and Maslin Bays is not at present known to have other planktonic
events suitable as a basis of zonation until Hantkenina alabamensis compressa
Parr is encountered in the lower part of Blanche Point Transitional Marts,
A zone of Clobigerina linaperta has its lower boundary defined by the top
of the local range of Turhvrotalia aculeata and its wpper by the top of the rouge
ol GC, linaperta s.str. This is comparable with the G. Iagperke zone of Jenkins in
the upper Kaiatan and Runangan of New Zealand, but there he shows the final
appearance of G. linwperta to be contained within the basal part of his brevis
zane which is not yet recognized in Australia, Species associated with G. lina-
verla in this adapted linaperta zone inelude Chiloguembelina cubensis, Casst-
gerinella sp, ct ©, chipolensis, Turborotalia increbescens, Globigerina aniplia-
pertuea, G. angiporoides angiporvides, and, at the top, Guembelitria stavensis
apd Globigerina cuapertura, The zone of Gy linaperta is present in the upper-
most part of the Aldinyan.
The zone of Chiloguembelina eubensis has its lower boundary defined by
the top of the local range of G. linaperta and its upper boundary by the final
appearance of C. cubensis. Species associated with the zonal specivs include
Guembelitria stavensis, Cassigerinella chipolensis, Globigerina enapertura, and
very rare and doubtful specimens of G. engiporvides angiporoides. Also occur-
ring towards the top ot the zone in the type section are Globigerina bulloides
dOrbigny, G. sp. ef. G. ciperoensis cipéroensis Rolli, G. lablacrussata Jenkins,
and Globorotaloides. testarugosa (Jenkins). A specimen of Globanomalinu sp. of,
G, naguewichiensis (Myatliuk) was recovered from the top of the zone, The
zone of C, cubensis is pust-Aldingan, and its uppermost part, at Jeast, is early
Janjukian. ‘Ihe zone is likely to be synchronous with most of the brevis zone,
the whole of the angiporoides angiporvides zone, and the basal part of the
euapertura zone of Jenkins.
The zone: of Guembelitria stavensis has its lower boundary defined by the
top of the local range of Chilozuembelina cubensis, and its upper boundary by
the final appearance of the zonal species, the latter event almost certainly
occurring stratigraphically higher than the top of the type section of Port Wil-
linga Beds, In the Willimga Bore W.B1, and generally in the Adelaide Plains
Sub-basin, G. stavensis ranges up above C. cubensis (Lindsay, 1968, 1967, cited
above). At the top of the type section the zunal species is associated with
Cassigerinella chipolensis and Globieerina bulloides. The zone would no doubt
eceupy ao interval in the lower part of Jenkins's evapertura zone (though Jenkins
does not record G, staversis), in uppermost Whaingaroan and perhaps basal
Duntroonian.
FORAMINIFERA
PLANKTONIC Species
Throughout the type section, planktonic species are mostly small and re-
stricted im variety, although at tmes abundant, No reworking is apparent, The
local rauges of more significant species are plotted in Fig, 2,
Globigerina praebulloides (many comparable with subsp, leroy! Blow and
Banner), G, angustinmbilicata Bolli, G. officinalis Subbotina, and G, ouachittaensis
Howe and Wallace, range through the sequence, comprising an association of
stnall, apparently tolerant, species related to the Globigerina bulloides Lineave
which was discussed by Wade. They often form the mest obvious and abundant
FORAMISIFERA AND STRATIGRAPHY OF PT. WILLUNGA BEDS 1M]
planktonic vornponent of the samples examined and appear to be typically
presen in Upper Eocene and Oligocene sequences elsewhere. Because of their
ong ranges, however, they are omitted from Fig. 2.
Guembelitria stavensis Bandy
Pl. 1, Fig. 1
1949, Cuembelitria stavensis Bandy, Bull. Am. Paleont., 82 (131), pp, 124-125, pl. 24, figs.
aD,
1964, Guembelitria sp.; Wade, Micropaleontology 10 (3). pp, 286-287, pl, 1, figs. 12a-b.
The South Australian species of Guembelifria which occurs in the upper-
most Eocene and Oligocene, has been compared with the types of C. stavensis
kindly loaned by the University of Indiana, At Port Willunga, the species com-
reces its range about 7 feet (2 m.) below the extinction of Globigerine linaperta
and continnes up to the top of the section beyond the highest occurrence of
Jhileguembelina cubensis, this latter part of its range comprising the basal part
of the zone of G. stavensis. The species has a wide distribution in the St, Vincent,
Murray and Otway Basins,
Chiloguembelina cubensis (Palmer)
Vi. 1, Figs, 2-3
1934. Giimbelina cubensis Palmer, Mem, Soc, Cubana Hist. Nat, 8 (2), pp. 74-75, teat figs.
1-6 (fide Fllis and Messina, 1940 ef seq, ),
1957. Chilovwembeliza cubensis; Beckmann, Bull, U.S. Natu, Mus, 215, pp, 84, 89, pl. Qt,
fiz. 21, text tig, 14 (5-8).
(984, Chiloguembelina rosa, Wade, Micropaleontalogy, 10 (3). pp. 286-287, pl. 1, fi. 2.
Beckmann (1957) commented on the stratigraphic usefulness of Chiloguem-
helina, particularly in samples containing mainly a benthonic fauna, and his
remarks are supported by the writer's experience of both Chiloguembelina and
Guembelitria in the Upper Eocene and Oligocene of the Murray and St. Vincent
Basins in South Australia,
Reynolds (p. 129) was the first to note the presence of “Gumbelina” in type
Port Willunga Beds, from sample A.114, 18 feet above the base of the formation
(Carter, 1955, p. 25). It is now known that C. cubensis ranges almost through-
out the section, appearing to approach extinction towards the top in basal
Janjukian equivalents, where it becomes very rare and sporadic. The last-
appearing specimen is figured.
Resides Carter's record of the last appearance of the species itn Faunal
Unit 4 low in the Jan Jue Formation at Bell’s Headland (Carter, 1964, p. 42,
fiz. 14), Taylor (1966), records C, cubensis above G. linaperta trom Esso Gipps-
land Shelf No. 1 Well in his Zonule | which he compares with Faunal Unit 4.
Jenkins puts the extinction of C. cubensis within the basal part of his euapertura
zone, high in the Whaingaroan of New Zealand. Ue has recently (1966) made
this extinction the eleventh in a series of twenty-nine homotaxial datum planes
ehosen hy hima tor the Pacific and Trinidad Tertiary. In Trinidad, C. cubensis
makes its final appearance in the opima epima zone. The ooeurrence of this
datum plane near the top of stratotype Port Willunga Beds is thus of consider-
able importance. Although the planes are described by Jenkins as homotaxial
and not necessarily isochronous, he accepts the extinction of C. cubensis as an
Oligocene event.
Globanomalina sp. cf. G, naguewichiensis (Myatliuk)
PL 1, Figs. +5
1950, Globizerinella naguewichiensis, Myatliuk, Trad veces. aeft, nauchno-issled. geol-razy.
Inst, (VNIGRT), Mikrofaunw $.8.8.8., sb. 4, vyp, 31, 251, pl. 4, figs. 4a-b (fide Ellis
and Messina, 1940, et seq.).
102, J. M. LINDSAY
1982. Vee daheucbuertag naguewichiensts; Blow and Banner (University Press, Cambridge).
p. id.
Loeblich and Tappan (1964, p, © 665) are followed in regarding Pseudo-
hastigerine as a synonym of Globanomalina. A solitary small planispiral speci-
men with six chambers im the final whorl was recovered from the top of the
cubensis zone, It is Glohanomalina, apparently less akin to G. micra (Cole) than
to G, naguewichiensix (fide Ellis and Messina, 1940, et seq.). The extinction
of Myatliuk’s species, as the last-surviving species of Globanomalina, marks the
lower boundary of the hasel Neogene zone N.1 of Banner and Blow (1965 },
Too much importance cannot be attached to a single specimen, bul the vccur-
rence does provide some support for the widely-held view that the extinction
of G. cubensis oceurred in the Palaeogene and Oligocene.
Cassigerinclla chipolensis (Cushman and Pontor))
Pl. 1, Fig, 6
1932. Cassidulina chipolensis Cushman and Ponton, Bull, Fla, St geol, Surv. No, 9, q. 98,
pl. 15, figs, 2a-c (fide Fllis and Messina, 1940 ef seq.)
W683. Cassigerinella chinolensis; Blow and Banner (University Press, Cambridge), pp, 81, 83,
pl. XV (M,N) (synonymy).
Ae. poseerinete chipolensis; Wade, Micropaleonlology, 10 (3), pp. 286-287, pl, 1
ig. 22,
Specimens with well-developed biserial enrolling and prominent aperture,
occur through the cubensis and stavensis zones, The species ranges as ligh as
the Baleombian Munneo Para Clay in the Adelaide Plains Sub-basin, and up to
Bairnsdalian Pata Limestone in the Murray Basin of South Australia,
Cassigerinella sp, cf. C, chipolensis
PI. 1, Figs. 7-9
Blow and Banner did not find any forms referable to the genus Cassigerinella
in the Eocene of the Lindi area, Tanganyika. However, in stratotype Port
Willunga Beds, forms from the upper part of the aculeata zone, and the linaperta
zone, are referable to Cassigerinella and are compared with C. chipolensis.
Eleven such specimens have been recovered. They usually haye a distinct
planispiral early stage, but also display the biserial enrolling of € rassigerinelia,
In some examples the aperture tends to be more restricted and slit-like than is
the case with C. chipolensis, but the earliest form (pl. 1, figs, 7-8) hag a alis-
tinctly open oval aperture. The lowest sample south of Aldinga Creek with C.
sp. ct. C. chipolensis (155-66) also contains immature but characteristic Clobi-
gerapsis index index besides Turborotalia aculeala, The earliest C. sp. cf. C.
chipolensis in the type section is from sample 123-66 north of Aldinga Crévk,
and is associated with the latest Maslinella chapmani Glacssner and Wade.
Todd (1966, p. 14) hus recently discussed the possibility thal Cassizerinella
occurs in the Eocene. The evidence from Port Willunga Beds seems to confirm
that it does,
Turborotalia aculeata (Jenkins)
Pl, 1, Figs. 10-11
1963. Globorotalia inconspicua aeuleuta Jenkins, N-Z. 1, gool. geophys., 8 (8), pp. 1118, 1120,
fig. 13, nos. 129-125.
Tn the present study, nou-keeled Globorotaliinac are assigned to Turboro-
talia following Loeblich and Tappan (1964, p. C 668). This distinctive finely
spinose species described from the Bortonian and Kaiatan Stages of New
Zealand, is present, at times abundantly, in the basal 22 feet (6% m.) of the
type section, in the aculeata zone, Its differences from Cloborotalia inconspicue
Howe, noted by Jenkins, appear to sulfice for its transfer from a subspecios of
FORAMINIFERA AND STRATIGHKAPHY OF PT. WILLUNGA BEDS 4U3
G. inconspicua to a distinct species in Turborotalia. Both north and south of
Aldinga Creek, the highest oceurrence of JT. aculeata is in a green clay with
white limy nodules, sipporting the equivalence of these two beds as shown in
Fig, 2. The species is known from the Eocene of the St. Vincent, Murray, and
Otway Basins of southern Australia.
Turborotalia increbescens (Bandy)
Pl 1, Fig. 12
1949. Plodigetine increbescens Bandy, Bull, Am, Paleont, 32 (131), pp, 120-131, pl 2%
s. dat.
1962. Globorotalia (Turborotalia) inerebeseens; Blow and Banner (University Press, Cam-
bridge), pp. 118-119, pls. XUN (T-V). XVII (D, K), tig, 9 (xiii-xv),
15683. Racbaronlie increbescens; Reed, Bull. Am. Paleout,, 49 (220), pp. 86-87, pl 14,
vs. 11-13.
The species has been formd only in two samples straddling the top of the
aculeata zone north of Aldinga Creek. This is somewhat higher than the range
recorded by Jenkins from New Zealand, but is within the lower part of the
range recorded by Blow and Banner from Lindi (op. cit., Fig. 20).
Turborotalia opima continuosa (Blow)
Pl. L. Figs. 13-14
1959. Globorolalia opima ciintinuosa Blow; Bull. Ain. Paleont., 39 (178), pp. 218-219, pl.
19. figs. 125a-c,
1963. Cloborotalia continwosa; Jenkins, N.Z. J. gcol. geophys.. § (G6), fig. 2 (range chart),
Only two examples have been recognized, both from sample 145-66 at the
top of the cubensis zone, from a level near the bottom of the range of the species
as recorded for New Zealand by Jenkins. The specimen figured agrees closely
with Blow’s diagnosis of the subspecies, which by the criteria of Loeblich and
Tappan belongs to Turborotalia rather than to Cloborotalia,
Globigerina ampliapertura Bolli
Pl. 1, Fig. 17
1057. Globigerina anpliapertura Bolli, Bull. U.S. Nati, Mus, 215, p. 108. pl. 23. figs. 4u-7b,
1962, Globigerina amplianeriure anpliapertuya; Alow anc Banner (University Press, Cam-
bridge). pp, 83-84. pls. XT (A-D), XVIL (C), fig. 12b.
The species has heen seen only in the Aldingan portion of the type section,
mostly in the /inaperta zone, where it is small with a relatively high arched
aperture, This is comparable with the basal part of the range of the species in
New Zealand as recorded by Jenkins.
Globigerina angiporoides angiporoides Hornibraok
PL 1, Fig. 25
1965, Globigerina angiporoides Hornibrook, N.Z. J. geal. geaphys., 8 (5), pp. 834-838, figs.
1 (ai), 2 (synonymy). ;
1965, Glubizerina angiperoides angiporvides: Jenkins, NvZ. J. geol, geophys,. & (6), pp.
1092, 1096, fig, 3. (range chart).
Through the aculcata zone this form oceurs typically and consistently but
mostly very rarely. Tt ranges into the fingperta zone and occasional doubtful
examples are present nearly le the top of the evbensis zone. Taylor (op, cit.)
recorded this species (as G. angipora Stache) only from his Zonule K of upper-
most Eocene age in Esso Gippsland Shelf No. 1 Well, associated with C, Tina-
peria. G. angiporoides angiporoides is abundant in the “Lower Clen Aire Clays”,
and as was noted above, there is litte doubt that it is the form referred to by
Carter as “G. linaperta with swollen chambers”, the characteristic species of
his Fauna) Unit 3 or “Jinaperta zone”,
14 J. M, LINDSAY
Globigerina bulloides dOrbigny
Pl 1, Fig. 16
1941, Globigerina bulloides @Orbigny; Cushman, Conir, Cushman Lab. foramin. Res., 17
(2). pp. 38-39, pl. 10, figs, 1-13 (synonyny ).
1959. Glabigoring bulloides; Blow, Bull. Am, Paleont., 8% (178), pp. 175-176, pl. 9,
igs, GSa-e,
There has been some disagreement among micropalacontologists over the
age of earliest G. bullvides, varying for example from middle Miocene (Blow,
1959, p. 175) to Upper Eocene (Wade, op. cit, p. 278), Jenkins recorded
earliest G. bulloides in New Zealand from middle Whaingaroan Stage ( Oligo-
cene). and comparable with this, in type Port Willunga Beds, forms attributable
to G. bulloides enter high in the cubensis zone and are prominent within the
Janjukian interval,
Globigerina sp. cf. G, ciperoensis cipcroensis Bolli
Pl. 1, Fis, 18
1954, Globizerine ciperaensis Bolli, Coutr. Cushman Pdn. foramit, Res,, 5 (1), pp, 1-2, text
fizs, 3, Sa. 4, 4a-b, 5, 5a-b. 6,
1957. Globigerina ciperoensis ciperoensis Boll, Bull, U.S. Nato. Mus,, 215, p. 109, pl. 23,
figs. 10a-h,
At a similar level to that recorded by Jenkins for New Zealand, the ciperoen-
sig form is emerging as an offshoot from the G. qngustiumbilicata population at
the top of the cubensis zone in Port Willunga Beds, as it devclops a more highly
trochospiral, five-chambered whorl, a slightly hispid test, and 4 more open
centrally-situated umbilical aperture tending to Jose its lip. The specimeii most
similar to G. ciperoensis ciperoensis is figured, but its umbilicus is still relatively
small, and an apertural lip is still slightly developed.
Globigerina euapertura Jenkins
Pl. 1, Fig. 15
1960. Globigerina evapertura Jenkins. Micropaleontology, @ (4). p, 351, pl. 1, figs. Sa-c.
1962. Globizerina ampliapertura enapertura, Blow and Banner (University Press, Clagnu-
bridge). p. 84, pl. XT (E+G),
Commencing its range near the top of the Aldingan, G. euapertura oceurs
most frequently in the Janjukian interval. The rather low, rimmed, widely-
arched aperture and depressed final chamber, are distinctive features. Blow
aud Banner discussed euapertura as a subspecies of G. ampliapertura, and
showed its emergence from that lineage near the top of their turritilina furri-
tilina zone (uppermost Eocene) at Lindi. Similarly in New Zealand, Jenkins
records the commencement of the range of G. euapertura near the Runangan-
Whainyaroun boundary, At Port Willunga, sample 147-66 from just below the
top of the Aldingan Stage contained the specimens figured of the carliest definite
C. euapertura and the latest G. ampliapertura seen.
Globigerina labiacrassata Jenkins
Pl, 1, Figs, 20-22
1965, Globigerina labincrassata Jenkins, N.Z. J, geol. geaphys,, 8 (6), pp. 1102, 1104, 11086,
fig: 8 nos, 64-71,
A few examples of the species have been recovered from samples 9-67 and
13-67 in the upper part of the cubensis zone, ata level equivalent to the middle
of its range in New Zealand. The forms have moderately thickened apertural
rims, and variable size and height of aperture, as compared with the morc
typical figured specimen from the Otway Basin,
FORAMINIFEBA AND STRATIGRAPITY OF PT. WILLUNGA BEDS 105.
Globigerina linaperta Finlay
Pl, 1. Figs, 23-24
1939, Glahigerina linaperta Finlay. Trans, R. Soc. N,Z,, 69 (1), mp. 125. ph 15, Ags. £4-57.
1962, Globizerina linaperta linapertay Blow and Banner (University Press: Cambridge),
pp. 35-87, pl, XI (TL) (synonymy).
The apparent environmental tolerance of this species makes it stratigraplie-
ally important in Eocene correlation, Blow aud Banner demonstrated its
extinction at Lindi at the top of their furritilina turritilina zone, in beds sHll
Eocene on the evidence of diagnostic larger foraminifera such as Discocyclina sp,
For New Zealand, Jenkins recorded both G, linaperta and Globigerapsix index
index as haying become extinct at the top of the Runangan, and accepted this
as the Hocenc-Oligocene boundary, McTavish (1966, p. 16) maintained that
G. linaperta “persisted into the Oligocene in Australia”, while acknowledging,
its geveral extinction at the close of the Eocene, However. it seems likely from
present studies that Australian records ot G. linaperta from the Oligocene refer
vither to G. angiporoides angiporoides or to forms not conspecific with G.
linaperta but comparable with it in some aspects, The specimens figured from
Port Willunga Beds show the diagnostic features of the species. and in particular
the specimen from sample 148-66, the uppermost recovered, is very comparable
with New Zealand material examined,
Globorotalsides testarugosa (Jenkins)
PY, 1, Fig. 26
1060. Globorotalia testaruzosa Jenkins, Micropaleontology, 6 (4), p. S68. pl. 5. fin Baec.
1085. Cloborotaluides testarugesa: Jenkins. N.Z. J, geol, ycopbys. 8 (6), p. 1092, fig, 2
(range chart),
Good examples are present very rarely at the top of the cubensis zone,
equivalent to the middle of the range recorded by Jenkins from New Zealancl,
He described the species from the hase of the Lakes Entrance Oil Shaft in
Victoria at the top of its range. The form has also been recorded by Taylor
(op. cit.) from Esso Gippsland Shelf No. 1 Well. The figured specimen shows
the characteristic coarsely pitted wall and relatively straight tangential sutures
on the spiral side.
Globigerapsis index index (Finlay)
PI. 1. Fig, 19
1930. Globigerinoides index inlay. Trans. R. Soc. NZ, 69 (1), p. 125, pl. 14. figs, 85-88.
1957. Globigerapsis index; Bolli, Bull. U.S. Natu, Mas, 215, p, 165, pl. 36, figs, 14a-J8b,
1965. Globigerapsis index index; Jenkins, N.Z, J. geol. genphys., 8 (6), pp. LO91, 1094. dig. 2
(range chart).
Immature examples with wide single apertures, as shown in the figured
specimen, occnr very rarely within the aculeata zone, Jenkins does not record
Globigerapsis tropicalis Blow and Banner from New Zealand and ranges hoth
G. index index and Globigerinu linaperta to the top of the Runangan. G, index
index is evidently more affected by adverse environment than is G. linaperta
and its usability as a zonal indicator is thereby lessened. However, its ovva-
sional presence within the bottom 16 feet (5 m.) of the type section of Port
Willunga Beds confirms the Upper Eocene age of this interval.
BeENTIIONIC SPECIES
The benthonic foraminifere have not been studied in detail and many of the
species are as yet undescrihed. A few of more immediate stratigraphic signifie-
ance will be noted here.
1G J. M. LINDSAY
An interesting assemblage is prescrit as a wumerically minur constituent of
the microfauna in the hasal 20 feet (6 m,) of the type section, within the Upper
Encene aculeaia zone, The members of this assemblage are: Crespinina Kings-
evlensis Wade, Linderina sp. Hulkyardia sp, cf. 11. bartrumé Parr. Maslinella
ehapmani Claessner and Wade, Reussella finlayi Dorreen, and a genus close to
Bolivinella, Their sanges within the type section are plotted in Fig. 2.
All South Australian specimens of Crespinina kingscotensis recorded by
Waile in her description of the species (1955), came from Eocene beds, It has
in addition been recorded by Ludbrook from Buccleuch 4, and B in the Murray
Basin (1961, Table X), and at Aldinga Bay (1956, p. 17) from as high as basal
Fort Willunga Beds, In South Australia it is thus only known as an Eocene
species,
Linderina sp., and Halkyardia sp. cf. H. bartrymi, have been recorded by
Ludhrook, and the latter figured, from Buccleuch A (1961). She has also noted
them (1963, pp. 8, 9) from other calcareous sediments in the U pper Eocene of
South Australia,
Maslinelle. chapmani is ouly known from the Eocene, Glaessnet and Wade
(1059) described South Australian occurrences from Upper Eocene beds at
Maslin Bay, Port Noarhinga, Kimyscote (Kangaroo Island), and Moorlands,
Ludbrook noted the species from Buecleuch A in the Murray Rasin (1961), and
in 1963, in Middle and Upper Eocene microfaunas from South Australia, inelud-
ing the Eucla Basin. A few examples have now been recovered from. the
weuleata zone in type Port Willumga Beds north of Aldinga Creck.
A genus closcly related to Bolivinella was recorded and figured by Lud-
brook (1961) frown Upper Eocene Ruecleneh A in the Murray Basin, and noted
by ber (p. 86) to occur assoriated with Mantkenina alubamensis compresse in
Blanche Point Transitional Marls at Maslin Bay. A fow glanconitie internal
tasts of the form have now also heen found at the top of Chinaman’s Gully
Beds in sample 118-66, and typical examples oceur Jaw inv Port Willunga Beds.
In a few of the specimens some coiling of the initial chambers has been ob-
served. This species is only known from the Rocene of South Australis.
As with the planktonics, these henthonies do not appear to have been
reworked from older beds, Occasional specimens show. slight wear, iuter-
preted us due tothe kind of contemporaneous abrasion which night he expected
in beds such as the basal cross-hedded bryozoal sands.
The assemblage noted above thus supports the planktonic evidence far an
assignment of Upper Kocene age to the aculeata zone in type Part Willunga Beds,
Cihicides pseudaconvexus Parr, 1938, rangus throughout the section but
vevurs only oecasionally above the aculeela zone, the uppermust example heing
Inund at the lop of the enbensiy zone. The species was reported by Carter to
be present as high as Paunal Unit 4 (1958, Table 8; 1964, Table 3),
Althongh mifiohds arc scarce in the type section, a single good example
of Maysilinu torquayensis (Chapman, 1922), was found at the top of the cubensis
zone, within the Janjukian interwal. A comparable finely striate siliceous internal
cast was recovered frum low in the cubensis yone, This is a characteristic
species of the Jan Jue Formation and its South Australian correlatives. A
specimen from the Ettrick Formation has been figured by Ludhrook (1961,
Pl I, big, 3).
Placed for the present in Notorvtalia, a species which is probahly mew
appears in the Janjukian near the top of the eybensis zone, It ranges up into
PORAMINIFERA AND STRATIGRAPHY OF PT. WILLUNGA BEDS LaF
the stacvensis zone, and elsewhere into the basal Miocene of the Murray aod St.
Vincent Basins. More robust, and somewhat Jarger Uian Notorotalia howehini
(Chapman, Parr and Collins), it has a more or less pronvinent but flush um-
hilical plug. It is quite distinct from Porosorotalia crassimura (Carter), which
is present throughout the type section,
Pseudopolymorphina rutile parri Cushman and Ozawa, 1930, has only been
seen trom the top of the ctibensis zone, It was deserihed from the Jan Juc
Formation and occurs sparsely in Janjukian correlatives in the Murray aud St.
Vincent Basins.
Sherbornina atkinsoni Chapman occurs throughout the type section, pre-
ferring calcareous sandy facies, but S$. cuneimarginafa Wade is not present,
Notably absent from even the Upper Eocene part of Port Willunga Beds
are Asterigerinella aclelaidensis (Howchin) and a distinctive, striate, Pseudo-
polymorphina sp. (of Ludbraok, 1961, Pl. 1, Fig. 1), In the St. Vincent Busin
the former is not known from above Blanche Point Marls and the latter ranges
no higher than the Blanche Point Transitional Marls Member.
Victoriella conoidea { Rutten) has not been seen in the type section, and
in any case use of the Victoriella conoidea zone (Carter, op. cit; “V. plecte”
zone of Glaessner, op. cit.) would be mappropriate for a scheme of planktonic
zonation. The cubensis and stavensis zones vt the present scheme are used
instead for all but the uppermost part of the zone of Victoriella conoidea, The
species has been found by the writer recently for the first time in the Adelaide
Plains in the Croydon Bore where it occurs in Port Willunga Beds at 1,040-
1,045 fect (817-319 m.) in pale brownish-prey limestone, 25 feet (7-6 m.) above
the top of the stavensis zone, and associated in an upper Janjukian microfauna
with Cibicides psuedoconvexus, Clubigerina sp, cf. G. angulisuturalis Bolli,
Massilina torquayensis, Sherbornina atkinsoni and Sherborning cuneimarginata.
This is above the level of the type section of Port Willunga Beds, and must be
close ta the Oligocene-Miocene boundary.
ACKNOWLEDGMENTS
Grateful acknowledgment is made of guidance by Dr, N. H. Lndbrock,
Senior Palaeontologist, helpful discussions with Mr. W. K. Harris, Palynologist,
and technical assistance in photography by Mr, Harris and Miss L. Linke.
Laboratory Assistant. The drafting was done by Mr, D, C, Sutton, of the De-
partment of Mines Drawing Office, Dr. Iudbrock and Mr. Harris read and
criticized the text.
REFERENCES
Bannna, F, T. abd Brow, W. O. 1965, Progress iv the Planktonic Forasniniferal Bio-
stratigraphy of the Neogene. Nature, Lond.. 208 (5016). pp. 1164-1166.
Becxmamn, J, P., 1957, Chiloguembelina Loeblich and Tappan and Related Foraminifera
from the Lower ‘Tertiary of Trinidad, B.W.I. Bull, U.S, Natn, Mus,, 215, pp. 82-46,
Buow, W. H., 1959. Age. Correlation, and Biostratigraphy of the Upper Tocuyo (Sau
Lorenzo) and Pozon Formations, Eastern Waledn, Venezuela. Bull, Am, Paleont., 39
(178), pp. 59-251, pls. 6-19,
Biow, W. H.. and Banner, F, T,, 1962. The Mid-Tertiary (Upper Eocene to Aquitanian)
Globigerinaceae. Part 2 in Eames, F. E,, et al., Fundamentals of Mid-Tertiary Stratl-
graphical Correlation, viii + 163 pp., pls. LXVIT (University Press, Cambridge},
Canrer, A. N., 1958. Tertiary Foraminifera from the Aire District, Victoria. Bnill. Geal.
Surv, Vie., 55, 76 pp,, pls. 1-10.
Canren, A. N., 1964. ‘Tertiary Foraminifera from Gippsland, Victoria, and Ther Steati-
graphical Significance. Mem. geol, Surv. Vict., 23, 154 pp. pls. 1-17.
Crtaeman, F,, 1922. Report of an Examination of Material Obtained fron a Bore at ‘Torquay.
108 J. M, LINDSAY
Kev. geol, Surv, Viet. IV (8), pp. 315-324, pl. LL.
Eras, B. F., and Messiwa, ANcrnina, 1940. ef seq. Catalogue of Foraminiferuz. Am.
Museum Nat. History.
Guarssnen, M, F.. 1951, ‘Three Forantiniferal Zones in the Tertiary of Australia, Geol.
_ Mag. LXXXVIT (4), pp. 273-283.
GiArssNen, M, F., and Wave, Many, 1958, The St. Vincent Basin, 115-126, f@ Gnansssrn
tye? and Fastin, L. W. (ed_), Vhe Geology of South Australia, J. weal. Soe, Aust, 5
+), pp. 1-163.
Guagssnek, M. F., and Wane. Many, 1959, Revision of the Forammiferal Family Vic-
toriellice, Micropaleantolozy, 5 (2), pp. 193-212,
Jexxins, D. C., 1965, Planktonie Foraminiteral Zones and New ‘Taxa from the Danian to
Lower Miorene of New Zealand, N,Z. J. geol. geophys.. 8 (6), pp, 1088-1126,
Jexsrys, D. G.. 1066, Plauktonic Forsminiferal Datum Plancs in the Pacific and Trinidad
Tertiary, N.Z, J, yeol. geophys., 9 (4), pp, 424-427-
Luspsay, J, M., 1965. Immanuel College, Camden Park, Bore No. 1, Stratigraphy and Micro-
paltcontology, Geol, Sury. S. Aust. Pal. Rep, 14/65 (unpmblisbed ), ;
Linnsay, J. M., 1966, Stratigraphy ancl Micropalacontolopgy of the Willanga Bore W.B. 1 —
a Re-examination, Ceol. Sury. $, Aust. Pal. Rep, 8/66 (unpublished ).
Linpsay, J. M., 1967. Adelaide Plains Sub-basin Stratigraphy and Micropylaeontolouy,
Summary Report No. 4, Geol. Surv. S$. Aust. Pal Rep, 1/67 (unpublished),
Linpsay, ], M., and Sueparep, B. G., 1986. Munno Para Clay Member. Quart. geol. Notes,
geol, Surv. S, Aust, Nu. 19. hily, pp. 7-11.
Tornutcn, A. R., and ‘Tappan, TY. with others. 1964. Treatise on Invertebrate Paleontology.
Lt. C. Protista 2. Sarcodina, chielly “Theeamovbians” and Waraminiferu, 1, 2) axxi,
C1-900, (‘The Geological Society of America and The University of Kansas Press, )
Lvpskoox, N. H., 1956. Supplementary Note on Willunga Basin Sediments. Rep, livest,
weol. Surv. S, Aust. No. 8, Appendix, pp. 15-18,
Lunvuoox, N. H.. 1961. Stratigraphy of the Murray Basin in South Australia, Bull. seal,
Surv. &. Anst., 386, 96 pp, pls. 1-VIIT.
Lupwnoor, N. H.. 1963. Correlation of the ‘Tertiary Rocks of South Australia. "Trans. H.
Soc. $. Aust.. 87, pp. 5-15.
Lupunoox, N. Hard Linosay, J. M, (966, The Aldingan Stage, Quart. geol. Notes geal,
Surv, 5. Aust.. No. 19, July, 1, 2.
MeTavist, R, A,, 1966. Planktonie Toraminifera from the Malaita Group, British Solomon
Islands, Micropaleontology, 12 (1), pp. 1-36.
Pan, W. J., 1959. Upper Eocene Foraminifera from Deep Borings in King’s Park, Perth,
Western Australia. J. R. Sec, West. Aust. XXTV, pp, 69-101.
Kaccair, HW. G., ond Crespixn, 1. 1955, Stratigraphy of Tertiary Rocks between ‘Torquay
and Eastarn View, Victoria, Proc. R, Sus. Vict, (N.8.). 67 (1), p. 75-143. pls. FV-VUl
Reynowps, M. A,, 1953, The Cainozoie Succession of Maslin and Aldingn Rays, South
Australia. Trans. R, Soc, $. Aust., 76, pp, 114-140.
Tater, R. 1878. Notes on the Correlation of the Coral-bearing Strata of South Australia,
with a List of Fossil Corals Occurring in the Colony, Trans. Proc. Rep. phil. Sue.
Adel. for 1877-1878. pp, 120-133.
Tare, R., 1879. The Anniversury Address of the President. Trans, Prov. Kept. phil, Soc.
Adel, for 1878-1879, xxxix-lyxv. ; ‘
Tak, R., 1899. On Some Older Tertiary Kossily of Uncertain Age front the Murrav Desert,
Trans. R, Soc. S. Aust, 23 (1), pp, 102-111. pl. 1.
Tate, R. and Dennant, J.. 1896. Correlation of the Marine 'Cortiariog of Australia. Prt
fil, South Australia and Tasmania. Trans. R. Sov. S. Aust. 20, pp, 115-148.
Taston, D. J, 1966. Essa Gippsland Shelf No, 1, the Mid-Tertiary Foraminiferal Sequence,
Appendix 3, 31-46. In Publs. Petrol. Search Subsidy Acts Aust, No, 76,
Town, Rute, 1866, Smaller Foraminifera from Cuam. Prot. Pap, U.S. geol, Surv. 403-1,
41 pp., . L19,
Wanr be Peete A New Genus of the Chapmanininue from Southern Anstralia, Contr,
Cushinan Fdn. foramin, Res., VI_(1), pp. 45-49, pl. 8.
Wap, Many, 1964, Applicstion of the lincuge concept to biostralivruphic zoning based ou
planktonic foraminifera. Micropaleontolagy, 10 (3), pp. 273-290,
Mis.
Vig.
Fig.
FORAMINIFERA AND STRATIGRAPHY OF PT, WILLUNGA BEDS 109
. 17,
20-22.
23-24,
25.
26,
EXPLANATION OF PLATE
Puate 1 (all figures X 110)
All from type section of Port Willunga Beds except Pig, 22.
Guembelitria stavensis Bandy. Wypotype Ff419, sample 145-66, top of eiibensis
zone, Oligocene.
Chiloguembelina cubensis (Palmer). Hypotype I'f420, sample 145-66, as above,
2, Side view. 3. Oblique view showing aperture.
Globanomalina sp. cf. G. naguewichiensis (Myatlink). Hypotype Ff421. sample
145-66. as above. 4. Side view. 5. Apertural view.
Cassigerinella chipolensis (Cushman and Ponton). Hypotype Ff422, sample
144-66, high in cubensis zone, Oligocene. Side view, showing aperture.
Cassigerinella sp. of. C. chipolensiy (Cushman and Ponton), 7, $. Hypotype
Ff423. sample 123-66. genleata zone, Upper Eocene, 7, Apertural side view.
8, Oblique apertural view. 9. Hypotype F424. sample 126-66, top of aculeata
vone, Upper Eocene. Side view.
Turborotalia aculeata (Jenkins), Hypotype F425, sample 163-66, aculeata
zone, Upper Eocene, 10. Umbilical view. 11, Spiral view.
Turborotalia inerebescens (Bandy). Hypotype Ff426, sample 127-66. basal
linaperta zone, Upper Eocene. Umbilical view,
Turborotalia opima continuosa (Blow). WHypotype Ff427, sample 145-66, top of
cubensis zone, Oligocene. 13. Side view showing the “comma-shaped aperture”
noted by Blow. 14, Umbilical view.
Globigerina euapertura Jenkins. Uypotype F428, sample 147-66, near top of
linaperta zone, uppermost Eocene. Umbilical view.
Globigerina bulloides C@Orbigny. Wypotype PF429, sample 145-66, top of
cubensis zone, Oligocene. Umbilical view,
Globigerina ampliapertura Bolli, Hypotype Ff430. sample 147-66, near top of
linaperta zone, uppermost Eocene, Umbilical view,
Globigerina sp. cl. G. ciperaensis cineroensis Bolli. Hypotype Ff431, sample
145-66, top of cubensis zone. Oligocene. Umbilical view.
Globigerapsis index index (Finlay). Hypotype Ff432, sample 161-66, aeuleata
zone, Upper Eocene, Umbilical view showing single aperture of immature
specimen,
Globigerina labiaerassata Jenkins, 20. Hypotype F433, sample 9-67, high in
cubensis zone. Oligocene. Umbilical view showing relatively small aperture
with thick rim. 21. Hypotype F434, sample 13-67, cubensis zone, Oligocene.
Umbilical view showing larger aperture and thick rim, 22, Hypotype F435,
Oil Development N.L. Mount Salt Structure Hole No, 3, 560-570 feet, Gambier
Limestone, Oligocene, Otway Basin, 10 miles (16 km.) south-west of Mount
Gambier. Umbilical view showing typical apertural features,
Globigerina linaperta Finlay. 23. Hypotype F436, sample 120-66, aculeata
zone, Upper Eocene. Umbilical view, 24, Hypotvype Ff437_ sample 145-66,
top of linaperta zone, uppermost Eocene. Umbilical view.
Globigerina angiporvides angiporoides Hornibrook. Uypotype Ff438, sample
21E-64, high in aculeata zone, Upper Eocene, Umbilical view.
Globorotaloides testarugosa (Jenkins). Hypotype F439, sumple 145-66, top of
cubensis zone, Oligocene. Spiral view.
J], M. Linpsay Phare 1
A NEW SPECIES OF EREMOPHILA FROM SOUTH AUSTRALIA
BY ELIZABETH A. SHAW*
Summary
In this paper is described Eremophila hillii, a species so far known only from two collections made
near Ooldea, South Australia. It belongs to the section Stenochilus (R.Br.) Benth., but differs
markedly from the other species placed herein by its small obovate to suborbicular crenate leaves.
A NEW SPECIES OF EREMOPHILA FROM SOUTH AUSTRALIA
by ExizAserH A, SHAwW*
[Read 13 July 1967]
SUMMARY
In this paper is described Eremophile hillii, a species so far known only
from two collections made near Onldea. South Australia. Tt belongs to the
section Stenochilus (R.Br.)Benth., but differs markedly fom the other specics
placed herein by its small obovate to suborbicular crenate leaves.
Eremophila hillii E. A, Shaw, sp, noy.
Section Stenochilus { R.Br.) Benth., Fl.Austr.d(1870)27.
Frutex usque ad 70 em altus, intricate ramosus, habitu cumulatus, pilis
erectis, albidis vel griseis, mnltiramosis vel ste)latis vel + plumosis vestitus.
Rami plerumque cicatricibus foliorum delapsorum praediti; iuniores dense
tomentosi sed vestutiores glabrescentes. Folia matura ca. 7-10 mm x 4-8 mm,
dense tomentosa, spiraliter disposita ut videlur, versus apices ramorum dense
conterta, obovata ad obirullata vel suborbicularis, sessilia yel in petiolum
brevissimum anguslata, pleruamque ad apicem rotundata vel subacutata raro
acutala, raro integra plerumque crenata. Flores singulalim in axillis foliorum
summorum disposili; pedicelli ca. 2-3 mm longi dense tomentosi. Sepala 5
imbricata, post anthesin probabiliter non aucta; exteriora 3 ca, 5-2-7-0 mm
longa x 2-5-3:4 mm lata, ovata ad deltata ad apicem rotundata vel subacutata,
in superficiebus ambabus dense tomentosa; interiors 2, ca. 4:5-5-5 mm longa x
1-8-2-6 mm lata, plerumque ovato-lanceolata subacutata, extus dense tomentosa
sed intus basem versus glabrescentia, Corolla ca. 3-0-3-5 cm longa in vivo
rubra, in sicco cinnabarina ad lateritia vel interdum flavida, in statibus ambabus
intus pallidior; extus pilis brevibus glandulosis sparsis aequaliter praedita,
intrinsecus pilis alandulosis irregulatim sparsis. utringue base versus (sub
seamentis calycis) glabrescens; supra ovarium corolla subglobosa cxpansa deinde
parum. contracta el supra denno ampliata ct leviter arcuata; {obi labii superioris
4 vonsimiles longitudine, ca. 2-0-3-5 mm longi, triangulares (ci laterales interdum
oblique triangulares) acuti; labium inferius ca. 12-16 mm longum, loratum
reflexumque, plerumque subacutum, Stamina 4, inter se non valde diversa, ca.
3:0-4-5 mm, longe exserta, filamentis complanatis et pilis glandulosis aspersis
praecipue ad basem vestitis, Otarium ca. 2°3-3:5 mm longum, glabrum
oyoideum, biloculare ovulis 2 in quoque loculo; stylus ca, 3:8-4-5 cm longus
gracilis ct glaber, I'ruectus ignotus. Semina ignota,
Tlonoryeus: ca. 3 km north of Ooldea; 209.1960; F.Wilson 1795. Sandhills. Rounded
bush 2 lt, high, Hower rec. Leaves whitish. — AD 96131130!
Shrub to ca, TO em in height, intricately branched and mounded in habit,
covered with white or pale grey many-branched, stellate or = plnmose erect
* State Herbarium of South Australia, Adelaide.
Traus. Roy, Soc, §. Aust. (1967), Voi. 91.
112 ELIZABETH A, SHAW
Fig. 1. Eremophila hillii W. A. Shaw. A, dowering branch; B, flower with corolla remoyed;
C, entire flower—(ill ex Wilson 1793).
NEW SPRCIES OF EREMOPHILA 113
hairs. Branches usvally with rather conspicious leaf scars, the younger ones
densely tomentose, but the older ones glabrescent. Leaves ca. 7-10 mm x 4-5
iwmm when mature, densely tomentose, apparently in a spiral sequence, very
densely crowded towards the branch tips, chovate to obtrullate to suborbicular,
apex usually rounded to subacute, rarely acute, sessile or tapering into a very
short petiole, rarely entire usually crenate; midrib not visible above, shghtly
raised abaxially. Flowers single, in the axils of upper leaves; pedicels ca. 23
mm long, densely tomentose: Calyx segments 5, quineuncial, probably not en-
larged atter flowering; 3 outer sepals ca, 5+2-7-0 mm Tong x 2-5-3-4 mm_ wide,
ovate to deltate, at apex rounded to subacute, densely pubescent on both sur-
faces: 3 inner sepals shorter and narrower, ca. 4-5-5-5 mm long x 1-8-2-6 mm
wide, usually ovate-lanceolate, subacute, abaxially densely pubescent, but on
the inside glabreseent towards the hase. Corolla ca, 3-0-3-5 em long, in civo
bright red, in sicco deep pink to brick-red or sometimes yellowish, in both states
aler on the interior; exterior with sparsely and evenly scattered short glandular
aits, glabrescent towards the hase (under calyx), interior with scattered glan-
dular hairs, glabrescent towards the base; corolla expanded over the ovary, then
contracted and again expanded and slightly fared and curved above, 5-lobed:
the 4 lobes of the upper lip all + the same length, ca, 2:0-3-5 tm long, triangular
(the lateral ones sometimes obliquely so) and acute; the lower lip ca, 12-16 mm
long, deeply cut into the tube, ligulate and usually subacute, reflexed. Stamens
4, all + the same length, ca. 3-(-4-5 mm, much exserted, slightly fattened and
bearing scattered glandular hairs, especially near the base. Ovary ca, 2-5-3'5
min long, glabrous, + ovoid, bilacular with 2 ovules per locule; style ca. 3-8-4-5
em long, slender and glabrous, Fruit and seeds unknown.
South Australia: ca. 5 km. north of Ooldea; 20,9,1980; P.Wilson 1795. Sandhills, Rounded
bush 3 ft. high, ower red, Leaves whitish. — AD 96131130 (holotyjpus): 2 km south of
Ooldes; 21.9.1960; D. J. E. Whibley 753 — AD 96104227.
Distribution: FE. hillit is so far kuown only from these two cullections made
at Ooldea on the Transcontinental rail line, When these specimens were found
during a routine sorting of Myoporaceae I thought it possible that they had
somehow been introduced from Western Australia, but they belong to none nf
the described species from that State. It is likely that E. hillit may be found
ta ae cons af the rail line; this is an area in which very few collectors have
worked.
Discussion: E. hillit belongs to Sect. Stenochilus of Eremophila, a rather
small group; Kriinzlin {1929} who treated it as a yeuus, Slenochilus R.Br., dis-
tinct from Eremophila, included only 15 species. ‘They are well distinguished
from other species of Eremopliila (s.1.) by having the lowest segment of the
5-lobed perianth cut much more deeply into the tube (4-6 times) than do the
uthers so as to form a narrow tongue which is usually reflexed. 2k. hillii differs
most markedly from all these 15 species cited by Kriinzlin by having small obo-
vate to suborbicular crenate leaves.
So far as [ know, there has been described since 1929 only ane species of
Eremophila belonging te this section. This species, E, vireny C. A, Gardner
(1942) from Western Australia, differs from F. hillii in several respects, for
example, height (3-5 m), leaf shape and size (generally laneeolate and up to
7-3 cm long), and corolla colour and size (green, 1-3 cm long), E- maggilttc-
rayi J.M.Black (1926), included umler section Stenochilus in the key to Eremo-
wile in Black's Flora of South Australia (1957), was not known to Kriinzlin,
(at differs from E, hillii in having much longer (1-5-6 cm) narrow-lanceolate
leaves, smaller foral organs, and calyx segments valvate rather than quineuncial.
114 ELIZABETH A. SHAW
E, hillii seems to be most closely related to E, glabra (R.Br.) Ostenf,; in its
usually accepted delimitation E. glabra includes quite a wide range of forms,
many of which have a tomentum like that of E. hillii and flowers practically
indistinguishable from those of the Ooldea plants. However, plants of E. glabra
generally have leaves which are * lanceolate and 1-5-5 cm Jong; I have seen
none which approach the crenate, obovate to suborbicular leaves of E. hillii and
I believe that the recognition of the latter as a distinct species is warranted.
This species is named in honour of Mr. Ronald Hill of the Botanic Garden,
Adelaide, who has a wide knowledge of this genus and a keen interest in it.
ACKNOWLEDGMENTS
I wish to thank Mr. R. Hill for providing information about the appearance
of these plants in the field and Mr. L. Dutkiewicz for preparing the illustrations.
REFERENCES
Bentiram, G., 1870: Flora Australiensis 5. London.
Brack, J. ie 1957: Flora of South Australia, ed. 2, vol. 4 (revised by E. L. Robertson}
Adelaide,
KrAxzuin, F., 1929: Beitriige zur Kenntnis der Familie der Myoporinae R.Br. Feddes Reper-
torium. Beihefte. Bd. 54.
A CONTRIBUTION TO OUR KNOWLEDGE OF SOME MAMMALS FROM
INLAND AUSTRALIA
BY C. M. PHILPOTT* AND D, R. SMYTH*£
Summary
We record the positive results of 24 weeks of field work on the mammals of northern
South Australia and adjoining areas. Localities, notes on the natural history and some discussion of
the taxonomy of the species located are given.
We found the rare rabbit bandicoot, Macrotis lagotis Reid, in two areas. The marsupial mouse,
Sminthopsis crassicaudata (Gould), was moderately common near Birdsville and Oodnadatta.
There is evidence that it is more active in the early part of nights without moonlight. Two other
rarer species of Sminthopsis and Antechinomys spenceri Thomas were taken as solitary specimens.
We located the two rock wallabies Petrogale lateralis Gould and P. xanthopus Gray.
Near Oodnadatta, we found a native rodent, either Pseudomys (Pseudomys) minnie Troughton or
Ps. (Ps.) rawlinnae Troughton. Two groups of specimens of Pseudomys (sub-genus Leggadina)
were obtained, but not specifically identified. Ps. (Leggadina) hermannsburgensis Waite and the
northern hopping mouse, Notomys alexis Thomas, were moderately plentiful in and near
northwestern South Australia. N. cervinus (Gould) and a solitary specimen of WN. fuscus
(Wood-Jones) from in and near south-west Queensland, were recorded.
A CONTRIBUTION TO OUR KNOWLEDGE OF SOME MAMMALS
FROM INLAND AUSTRALIA
by C. M. Prmprorr*f ann D, R. Smvru®t
[Read 10 August 1967]
SUMMARY
We record the positive results of 24 weeks of feld work on the mammals
of northern South Anstralia and adjoining areas, Localities. notes on the natural
history und seme discussion of the taxonomy of the species located are given.
We tonnd the rare rabbit bandicoot, Maerofis lagotis Reid, in twa areas.
The marsupial mouse, Sminthopsiy crassicaudata (Gould), was moderately
common near Birdsville and Oodnadatta. There is evidence that it is more
autive in the carly part of nights without moonlight. Two other rarer species
of Sminthopsts and Antechinumys spenceri Thomas were taken ag solitary speci-
mens.. We located the two rock wallabies Petrogale lateralis Gould and P.
sxanthopus. Gray, .
Near Oodnadatta. we found a native rodent, either Pseudamys ( Pseudomys)
minwe Troughton or Py. ( Ps.) rawlinnae Troughton. Two groups of specimens
of Psendomys (sub-genus Leyeadina) were obtained, but not specifically identi-
fied. Ps. (Legzadina) hermannsburgensis Waite and the northern hopping
mouse, Notomys alexis Thomas, were moderately plentiful in anc near north-
western South Australia. N. cervinus (Gould) and a solitary specimen of
N. fuscus (Wood-Jones ) from in and near south-west Queensland, were recorded,
INTRODUCTION
As early as 1925, Wood-Jones documented the alarming decline of popula-
tions of many South Australian mammals (Wood-Jones, 1923-5). Finlayson
(1961) surveyed the Central Australian mammal fauna, and his conclusions
showed that this decline was continuing. Calaby (1963) suggested that six
marsupials and several native rodents from Australia were already extinct, and
that as many as fifty species were either close to extinction, or so little known
that no definite statement could be made,
It is generally agreed that if many of Australia’s mammals are to be kept
from extinction, urgent measures to conserve them must be undertaken. It is
also agreed that knowledge of their distribution and natural history is a pre-
requisite to their conservation.
With the aim of contributing to this knowledge, we surveyed the mammal
fauna of parts of arid Australia. In particular, we sought information on the
following seven rare marsupials: Myrmecohius fasciatus rufus Wood-Jones,.
Macrotis lagatis Reid, M, leucura (Thomas). Chaeropus ecaudatus (Ogilby),
Bettongia pencillata Cray, Caloprynmus campestris (Gould), and Onychogalea
lunata (Gould), We also obtained information about other mammals during
the search for these seven rare species.
* Royal Zoolovical Society of South Australia, Frome Road, Adelaide, South Atistralia,
+ Present address: P.O, Box 1, Aldgate, South Australia,
t Present address: Department of Genetics, Australian National University, Canberra,
Australian Capital Territory.
Trans. Roy. Soc. §, Aust. (1967), Vol. 91.
tle CM. PMMNPOTY axp D, BR. SMYTIE
METHODS
The areas involyed in this survey are vast, and our time was limited, This
forced up to rely particularly on information from local people. The aboriginal
people, and in particular the older men from the large reserves in the north-west
of South Australia and Central Western Australia, gave us valuable informution,
Several rodents, and the fattailed marsupial mouse, Sminthopsis crassi-
cantluta (Gould), were readily found and caught at night. The procedure we
adopted was to drive along roads or over other accessile country at abont 25
miles per hour, with the lights of our truck on low beam. Small mammals
within about 30 yards (27 metres) of the truck could often be seen. They
usually ran away from the lights, but when followed with a spotlight trained on
them, they often sought refuge in depressions or hehind grass tussocks. Here
they would crouch motionless, and could readily be approached on foot. They
were then caught with a net or by hand. This method was particularly effective
for S. crassicaudata, which cannot run quickly.
Observation of sign in the form of burraws, tracks and droppings is an
obvious method of locating some species, The form of a burrow is often a
clue to the species: which made it. "Kuns” of the northern hopping mouse,
Notomys alexis Thomas, and the sandy inland mouse, Pseudomys (Leggadina )
hermannshurgensis Waite, atten led to burrows. Aboriginals are particularly
adcpt at digging these out, This is a practical method for obtaining alive such
burrowing species as the rabbit handicoot, Macrotis lagotis Reid. Several species
of Notomys, Pseudomys, and Sminthapsis were taken in this way, We did not
use traps. However, it is possible that the setting of a large number of traps
on many nights may have revealed the presence of rarer, more cryptic species.
The older aboriginals of the Pitjantjatjara tribe (from the Blackstone Range
to the Musgrave and Everard Ranges), and the Nga:nyatjara tribe (from the
vicinity of the Wacburton Ranges}, have specific names for the mammals of
their country. We found that the use of these names amongst thern created
immediate interest, and helped us obtain information on localities and the natural
history of many species. The aboriginal riames of some of the species considered
below are recorded. They are spelt phonetically following Douglas (1964).
Measurements of lengths of head and body, tail, hind-foot (pes), and ear vf all
specimens were taken using the methods described in Wood-Jones (1923). All
ead specimens secured on this survey are preserved in the South Australian
Museurn under the registered numbers used below.
RESULTS
Between April and December, 1966, we spent 24 weeks in the field. F ig. 1
shows the route we followed. Special attention was given to the following
uteas: near Birdsyille (3 weeks), south of the Blackstone, Manu and Musgrave
Ranges (3 weeks), and near the Warburton Range (3 weeks).
We obtained intormation on the distribution and natural histury of the
following species of mammals. Where no mention is made of a Species pre-
viousty recorded from inland Australia, it may be assumed that no positive
records of it were abtained,
Order Onnrmopecenta
Tachyglossus acileatus (Shaw and Nodder), Echidna
Aboriginal Names; t{irilya—Pitjantjatjara; tjilkamata—~Nyga:nyatjara,
SOME MAMMALS FROM INLAND AUSTRALIA 117
Field Notes. We made no serious effort to locate the moderately plentiful
echidna. Aboriginals at four settlements (Fregon, Ermabella, Musgrave Park
and Warburton), reported that it was common in nearby pOey hills. Residents
of two stations cast and west of Lake Eyre reported seeing indisputable signs of
Tachyglossus recently. We obscryed tracks and faeces at Mt. Lindsay,
129°54’E, 27°02/S.
GLENGYLE Hs.
N.T. .
BIRDSVICL
MISSION
M
ys
evEzaRo fa, s
- Pig Ne ee cREER BORE
ODNADATTA
KILOMETRES
oo AUTHOURS’ ROUTE
SOUTH AUSTRALIA
Fig. 1. Map of South Australia and adjoining areas, showing the survey route followed by the
authors, and the principal place names mentioned in the text.
Order DIDELPHIA
Family DASYURIDAE
Sminthopsis crassicaudata (Gould), fat-tailed marsupial mouse
(Plate 1, Figure 1)
Aboriginal Name: Papalakuntalkuntalpa—Pitjantjatjara (probably a com-
pound name).
Localities. (i) Within 15 miles (24 km) of Birdsville, SW. Queensland;
139°21’E, 25°54’S: June 6-23, 1966; 7 females ( 9 ) and 12 males (¢);1¢ now
South Australian Museum registered number M 6398. (ii) Within 5 miles (8
118 C. M. PHILPOTT anv D. R. SMYTH
km) of Glengyle Homestead, SW. Queensland: 189°36’E, 24°47'S; June 11-19,
1966; 3¢ and 48. (iii) Wire Creck Bore, 20 miles (32 km) N. of Oodnadatta,
N. South Australia; 135°28’E, 27°16’S, July 9-August 16; 8 9 and 4 4:1 ¢
now M 6399,
Field Notes. Most of the marsupial mice were caught at night using a spot-
light. At Birdsville and Glengyle, they were found on open gibber plains and
on sand-ridges and the flats between these ridges. A sand ridge where many
individuals were caught is shown in Plate 1, Fig. 2. At Oodnadatta, we caught
them on a gibber-strewn and deeply cracked flat shown in Plate 3, Fig. 2. Occa-
sionally a marsupial mouse, secn in the spotlight, would seek refuge in a well-
used burrow Jess than 12 inches (30 cm) long and 4 inches (10 em) deep.
We obtained some indication of the most active period of S. crassicaudata.
Fig. 2 is a histogram showing the number of marsupial mice caught per hour
of searching, against the number of hours elapsed since sunset. To draw this
graph, we considered only those nights when one or more mice were caught.
The accurate time of sunset in astronomical tables for all these dates was deter.
mined, and all times were converted to local time. We did not search earlier
than one hour after sunsct or later than nine hours.
END OF ASTRONOMICAL TWILIGHT
—
Ls)
MICE CAUGHT PER HOUR OF SEARCHING
o t 2 3 4 5 6 7 8 9 10
HOURS AFTER SUNSET
Fig. 2. Histogram of the number of fat-tailed marsupial mice (Sminthopsis
crassicaudata) caught per hour of searching with a spotlight, against the
number of hours elapsed since sunset. No searches were made earlier than
one hour after sunset and Jater than nine hours. Each interval includes at
least three and a half hours of searching.
SOME MAMMALS FROM [NLAND AUSTRALIA 119
Fig, 2 shows a trend of decreasing numbers of mice being caught per hour
of searching with increasing hos after sunset, This suggests that marsupial
mice were most active in tho early evening. The end of astronomical twilight,
and the beginning of complete darkness was about 1 hour 25 minutes after
sunset. Although we searched on several agcasions hefore this time, we saw tio
active marsupial mice,
We caught S. erassicaudata on calm and on windy nights, and on clear and
on cloudy nights, Some association of success in locating mice and the presence
of moonlight is suggested by the following figures. Only twenty-two per cent
of our successful searching time was carried out under moonlight (7 ont of 32%
hours), Also, during these moonlight searches, we only caught eleven per eent
of the total mice secured by this method (4 out of 37).
All mice were weighed alive within 24 hours of capture. There were no
significant weight differences between localities, The mean weight of 19 males
was 13-2 + 0-18 em, with a range of 10% to 17 gm, For 18 females, the mean
was 13-9 + 0-34 gm, and the range from 10K to 19 gm. There was no signifi-
cant difference between the weights of the sexes (tj; ~ 1:02, 308 << P< 40%).
None of the females had pouch-young,
A photograph of the tracks left by a live captive is given on Plate 1, Fig. 8.
The mouse was running quickly for cover. ‘he prints left by the two front
foet aro the last two in cach series in the photograph. ‘The left and right front
fect do not regularly alternate as the leading foot, ulthough this does occur
in Fig, 3.
Sminthopsis larapinta Spencer, stripe head marsupial mouse
Locality, Wire Creck Bore, 20 miles (32 km) N. of Oodnadatta, N, South
Australia; 185°28’R, 27°16'S; July 7, 1966, 1¢.
Field Notes. ‘This marsupial mouse was caught under similar circumstanecs
tithe S. crassicaudata individuals from locality (iii) shown on Plate 3, Fig. 2,
and considered above. It lived sympatrically with them, and a male and female
S. crassicauclala were caught close by within 35 minutes of the time of capture
of this specimen. Jts weight on capture was 2] gm.
Sminthopsis species, unidentified
Locality. Fregon, NW. South Australia; 132°02’E, 26°47'S;, July 16, 1986;
1 ¢; M6366.
Field Notes. We dug this animal from a shallow burrow on a sand-ridge.
The burrow resembled those of Pseudomys (Leggadina) hermannsburgensis
Waite, a small rodent which was common in the area. Aboriginals from the
settlement at Fregon did not haye a specific name for this species. They gave
us oly Mie word “mingkiri”, a word used generally for all sinall mice. This
suggested that the animal was rare or particularly cryptic.
Taxonomy. This marsupial mouse was smaller and more delicately built
than. §. eressicaudata and S. larapinta. The flesh dimensions (given in mm)
were: Lead and body 70, tail 85, hind-foot 13, and car 16, Its weight on capture
was 10% am. ‘The skull dimensions (given in mm) were: greatest length 20-9,
basal length 20-4, zygomatic breadth 11-5, interorbilal 4-3, braincase breadth
8-9, palate 11-0, nasals 7-4 x 2-0, bulla 5°7, anterior palatal foramina 1-5, P4
approx, 2x P; and Ps,
Carcful examination of the pes and manus showed that the sole-pads had
an obvious longitudinal row of enlarged granules at their apex. Troughton
(1964) claimed that this was a diagnostic feature of the murina “complex”. He
120 C. M. PINLPOTT anp D, K, SMYTH
stated, however, “The fact remains that hecause of the acknowledged lack of
differential cranial characters it is impossible to provide objective diagnoses
of the typical and allied forms of murina al present,” Positive identification of
this interesting specimen will have to await further collections and comparisons,
Antechinomys spenceri Thomas, western hopping marsnpial mouse
Locality, 16 miles (26 km) W. of Glengyle Homestead, SW. Queensland;
139°22’E, 24°48°S; June 14, 1966; 1 ¢; M 6387,
Field Notes. We caught this marsupial mouse while spotlighting at night
on an undulating gibber plain. It did not have pouch-young, and weighed
19-5 gm on capture. The native rodent Notomys cervinus (Gould) was caught
eluse by using the same method and it is probable that these two superficially
similar species are sympatric.
Family NOTORYCTIDAE
Notoryctes typhlops Stirling, marsupial mole
Aborivinal. Names: itjaritjari—Pitjantjatjara; yitarutju—Nega :nyatjara.
Field Notes. We were told that specimens of this distinctive species haye
been obtained within the last five years in sand-ridge areas on Everard Park
Station, Musgrave Park Station (No. 16 bore), Curtain Springs Station (where
it may be more common) and west of Warburton Mission. Aboriginals. from
Fregon and Warburton said that it is not seen in winter. However, others dis-
puted this claim. Most suggested that this burrowing species comes to the
surface after rain, It is not eaten by aburiginals. It seems likely that the mar-
supial mole, by reason of its small size and cryptic behaviour, is more common
than is indicated by a general survey.
Family PERAMELIDAE
Macrotis lagotis Reid, rabbit bandicaot
(Plate 2, Figure 1)
Aboriginal Names: talku, ninu—Pitjantjatjara; ninu, matura—N va:nyatjara.
Localities. (i) 12 miles (19 km) SW, of Mt. Aloysius, Blackstone Rane,
Central Western Australia; 128°27’E, 26°06’S; November 9 and 14, 1966; 2 2;
1 2 now M6340. (ii) 7 miles (11 km) N. of Warburton Mission, Warburton
Range, Central Western Australia; 126°34’E, 26°02’; December 7 and 8, 1966;
2 9;1 2 now M 6397.
Field. Notes. The results of a field study of a population from locality (ii)
will be reported elsewhere.
This species was collected near Birdsville during 1957-59 (Mack, 1961 }.
We were told that it had not been seen there for about five years, Tlowever,
we obtained reports of sightings of a mammal which was probably M. lagotts
within the last two years from localities west of Glengyle Homestead, The only
area we visited where it seemed tu be moderately plentiful was near Warburton
Mission. None of the females had pouch-young.
Taxonomy. ‘The measurements made on live specimens as soon as prac-
ticable after capture are given in Table 1. General appearance and the above
measurements suggest that these specimens belong to the type subspecies M.
lagotis lagotis Reid.
SOME MAMMALS FROM INLAND AUSTRALIA 121
TABLE 1
Flesh measurements of four female rabbit bandieoots, Macratiz layotia,
from Central Western Australia
Juvenile 9, Adult ¥*, Adult 9, Adult 2
Blackstone Ra. | Blackstone Ra. | Warburton Ra. | Warburton Ra.
Date of capture 9, XT.66 14.XT.66 7.X1T.66 8.XII.66
Wt. on capture (gm) 400 700 960 8m
Head and body (mm) 310 320 330 320
Tail (mm) 180 190 230 220
Ear (mm) 70 85 90 85
Hind-foot (mm) 78 88 96 92
* M 6340
+ M 6397
Family MACROPODIDAE
Petrogale lateralis Gould, black-lanked rock wallaby
(Plate 2, Figure 2)
Aboriginal Name: waru—Pitjantjatjara, Nga:nyatjara.
Locality. Alkara, 90 miles (145 km) SW. of Mt. Woodroffe, Musgrave
Ranges, NW. South Australia; 130°30'E, 27°04’S; July 27, 1966; 1 4 M 6388
(skull only).
Field Notes. We observed two or more rock wallabies on a rocky hill of
tumbled, granite-like boulders shown on Plate 2, Fig. 3. They emerged from
their Jairs at about mid-afternoon. The testimony of aboriginals that this wallaby
does not drink regularly was borne out by the absence of permanent water
nearby. Herbs and shrubs growing on the slopes, and which were possible
food species, included buckbush (Salsola kali), wild geranium (Erodium cyg-
Nora: several perennial grasses, and the shrubs Sida virgata and Ptilotus
obovatus.
Occasionally, aboriginals living on settlements from Fregon to Warburton
Mission catch and eat rock wallabies, and suggest that it is one of the more
plentiful mammals of the area.
The wallaby weighed 4-590 kg on capture, and its body dimensions (in
mm) were: head and body 525, tail 540, hind-foot 142 and ear 66.
Petrogale xanthopus Gray, yellow-footed rock wallaby
Field Notes. We observed these wallabies on April 10 to 16, 1966, at three
localities in the Northern Flinders Ranges between 138°40’ and 139°20’E longi-
tude, and 30°20’S and 30°40’S latitude, In two areas, we watched them feeding
on the green herbs in creek beds at dusk and at dawn, One female had a large
jocy.
Order MonopDELPHIA
Family MURIDAE
Psendomys (Pseudomys) species, unidentified native rodent
(Plate 3, Figure 1)
Locality, Wire Creek Bore, 20 miles (32 km) N. of Oodnadatta, N. South
Australia; 185°28’E, 27°16’S; July 9 and August 16, 1966; 4 9,3 3 and 8
juveniles (J); 1 @ now M 6341.
123 C, M. PHILPO'T axp D, R, SMYTH
Field Notes. ‘These native rodents were living on an open gibber flat, with
silver saltbush (Atriplex rhagodioides) heing the only perennial plaut. The
habitat is shown on Plate 3, Fig, 2, We dug eight of them from burrows built
under or near the saltbushes, “These burrows were less than 2 feet (60 cm)
long, and one is shown on Plate 3, Fig. 3. A male, a female and three juveniles
were dug from one burrow; another contained a male and a female, whilst a
third contained a solitary female. A male and a female were caught with a
spotlight about 4% hours after sunset on different nights. One of the females
captured on July 9 produced a litter of 3 on about July 12. She was paired on
October 21, and produced another litter of 8 on December 2. On January 3,
1967, she again produced young; this time there were 4 offspring.
Taxonomy. Tables 2 and 3 present flesh and skull dimensions of three of
these native rodents, and of types of Ps. minnie Troughton and Ps. rawlinnae
Troughton taken from Troughton (1932),
TABLE 2
Flesh dimensions of three adult: females ofan unidentified Pseudomys (Pacridomys) species from.
near Oodnadatta, N. South Australia, and of type specimens of Ps. minnie and Py.rawlinnae.
i
@, MB341 | 9, M6342* | 9, M6343") G, allotype 3, holotyps
Psominnie Ps. rawlinnne
Wt, ont capture (gm) 33 = ba —— =
Head and body (mm) EH) 8 101 117 113
Tail (mm) fn 85 93 111 oP
Ear (mm) 23 21 22 23 214
Hind-foot (mm) 26 24 27 27 2Tt
* Born in captivity, and measured when 6 months old.
TABLE 3
Skull dimensions (in pin x 10) of three adult fernales of an unidentified Pseadomys (Pseudamys)
species from near Oodnadalta, N, South Australia, and of type specimens of Ps. minnie and
Pa, rawlinnac.
i
|
9, M6p4L 2, M6a42* = | Oo, M6343* Pallotype | ¢ holotype
Ps. minnie Pa. rawlinnae
Greatest ieneth 29-5 28-4 | 20-4 307 BO-8
Baza! length 26-6 25-1 | 28-8 25-0 —
Zypomatic breadth | 15-4. 14-6 11-5 16-8 1u-L
Brainease bread 14-1 12-9 13-7 14°3 | 13-7
dnterorbital breadth 4-6 a-8 4s3 4-0 ars
Nasals length JL-4 LO-8 11-2 1-1 12)
Nasals hreadth 3-3 3-0 neh 3-0 2g
Palatal lungth 16-6 TA-4 16-8 14-0 14:5
Anterior palatal foramina 6-8 +7 67 7-3 TO
Bulla, a2 4-3 5-0 —
Upper molar series Gt 5-3 523 a-$ 5-a
Breadth M1 1-8 1-9 1-8 1:8
* Born in captivity, and measured when 6 months old.
We have used Tate (1951) to assist in the following deductions,
The absence of accessory cusps anterior to the first Joph of ml, and the
large size of the species indicate that it may be assigned to the sub-genus
Pseudomys Gray.
SOME MAMMALS FROM INLAND AUSTRALIA 123
The above tables show that the dimensions of our series are similar to those
given by Troughton (1932) for Ps. minnie and Ps. rawlinnae. The coat also
appears to be similar. Finlayson (tonite) noted that these species were similar
jn some features, but that the upper molar row, anterior palatal foramina, and
palatal length were shorter in Ps. rawlinnae. These differences are slight in
Table 3, but they may indicate that our series are closer to Ps. rawlinnae. Trough-
ton (1932), in his description of Ps. rawlinnae, made no mention of a black
caleaneal patch which is well marked on our specimens, However, Finlayson
(1939b) reported that the patch was present in the specimens he called Ps.
vawlinnae.
J. A. Mahoney of Sydney has examined these specimens. and_has indicated
that he considered the sum total of characters to be closer to descriptiuns of
Ps. minnie. However. he also noted that recorded descriptions of the two species
are little different, and that they may perhaps be shown after further study to
be canspecitic.
Pseudomys (Leggadina) species (group 1), unidentified native rodent
(Plate 4, Figure 1)
Localities, (i) 30 miles (48 km) N. of Birdsville, SW, Queensland;
139°28’E, 25°23'S; June 12, 1966, 22: M 6350-1, (ii) Wire Creek Bore, 20 miles
(32 km) N, of Oodnadatta, N, South Australia; 135°28’E, 27°16’S; July 9, 1966,
1 3; M 6352.
Field Notes. The two specimens from locality (i) were obtained by spot-
lightiny: about 7 hours after sunset. The single specimen from locality (ii) was
taken rom a shallow burrow, which was without a nest, and which had been
freshly dug after rain. The habitat at locality (fi) is shown on Plate 3, Fig. 2.
A series of tracks of a live captive from Birdsville are shown on Plate 4, Fig. 2.
The mouse was running for cover,
Taxonomy. Tables 4 and 5 contain skull dimensions of these three native
rodents, and also of types of Ps. forresti Thomas, Ps, waitei Troughton and Ps.
messoria Thomas taken from the original descriptions,
TABLE 4
Flesh dimensions of three adult males of on unidentified Pendomiys (Leggadina) species (group 1),
and of type specimens of Ps. forresti, Ps. watei and Py, measoria.
ls. M6350" | J, MG341* | 3, Ma3s2t| Gtype holotype, 3, type
\ Ps. forresti| Ps. welted [Pavnessoria
Head and body (mm) 80 76 83 a7
Tail (mim) 56 60 oo ad
Kar (mm) 12 Il 12 13
Hind-fuot (mom) 18 17 164 7
* From 30 miles N. Birdsville, 5.W. Queensland.
ft From near Godnadatia, N. South Australia; weighed 18-5 gm on capture.
The general characteristics of the skulls of these specimens fit Thomas
(1910) definition of the subgenus Leggadina. The specimens readily fit into
the forresti-vaitei-messoria group of Tate (1951), who provides a key to the
groups of Leggadina, The measurements above indicate that our specimens are
considerably smaller than Ps, forresti, but larger than Ps, messoria. Flesh dimen-
sions match those of Ps. waitei, but there are a number of differences, notably
the palatal and nasal lengths of the skulls. Coat colours of all three species in
124 C. M. PIILPOTT anv D, RK. SMYTH
TABLE 6
Slrull dimensions of three adult mules of an unidentified Psewdomya (Leggadina) species (group 1),
ant of typy specimens of Ps. forresti, Ps.waitel, and Fe. messoria.
Ss SSS
3, M6350" | 3, MG351*|3, M6352t] }, type |g. holotypel gy type
Ps. forresti| Ps. uxeites |Ps.mesaaria
Geeatest length 23-1 24-4 25:1 25-0 22-6 2a+5
Basal length 20-6. 217 21-5 — — —
Zygomatic breadth — 13-3 Lb. 1 13:5. 12-0 13-6
Rraincase breadth 11-3 11-7 11:6 — Shel 11-2
{nterorbital broadth Hei de6 ob: 7 oeé 3-5 3-6
Nasals Jength RS 8-3 h-4 8:5 7-6 8-0
Nuasals breadth 2+ 2-8 Beh = 2-3 —
Pulatal length 12°9 134 13-1 13-00 6] Jing 11-5
Anterior palatal foramina 5rl aes 4-9 5-5 3-3 4-0
Bulla — 4-2 42 — — 4-1
Upper molar series 405 405 4-4 4-4 4-1 4-5
Breadth M1 1:5 15 1l+4 — =~ —
|
ee ee es See
* From 31) miles N. Birdsyilly, &.W. Queensland.
$+ Frorn near Oodnadatta, N. South Anatralia.
the group, and of our specimens are apparently similar, However, Thomas
(1910) said that the hairs on the belly of Ps, messoria were slaty grey, whereas
tliose of the above series are pure white to the base,
Pseudomys (Leggadina) species (group 2), unidentified native rodent.
Aboriginal Name: ilpalya—Pitpantjatjara.
Localities—(i) 20 miles (82 km) SSE, of Mt. Aloysius, Blackstone Range,
Central Western Australia: 128°44°E, 26°17’S; November 15, 1966; 1 9 and 3]:
M 6344. (ii) 26 miles (42 km) SE. of Mt, Aloysius, Blackstone Range, Central
Western Anstralia; 128°52’E, 26°18’S; November 15, 1966; 4 2.14 and 11];
M 6345-9,
Field Notes, We dug these mice from burrows in two loamy plains near
rocky hills shown on Plate 5, Figs, 3. and 4, There were many small saltbushes,
grasses and ephemeral herbs on both plains, hut no other perennial plants. The
burrows were about 6 inches (15 em) deep and 15 inches (87 cm) long. A
nest of grass and fowers of an everlasting daisy was found in the deepest part,
One or more blind tunnels led from the nest. Unlike the unidentified Pseundomys
(Pseudomys) species, adult males and females were not found in the same
burrow, Two burrows contained solitary mice; one a malc, the other a pregnant
female. Four burrows each contained a lactating female and her young. ‘There
were two litters of three and two of four mice.
Living sympatrically with these rodents was the house mouse, Mus musculus
Linne. We dug out two pregnant house mice from burrows near to and closely
resembling those of the native mouse,
Pitjantjatjara_ elders from Musgrave Park unhesitatingly called the native
mice “ilpalya’. Finlayson (1961) reported that this was u Pitjantjatjara name
for a Notomys species “close to alexis but not specifically identified”.
Taxonomy, Tables 6 and 7 give measurements of individuals in the flesh
and of skulls of this series.
We have considered this group of specimens separately from the preceding
group of Pseudomys. Closer study may show them to be conspecific. As with
Pseudomys (Leggadina) species ( group 1), they fall readily into Thomas’ (1910)
subgenus Leggadina, and Tate’s (1951) forresti-waitei-messoria group.
SOME MAMMALS FROM INLAND AUSTRALIA 125
TABLE 6
Flesh dimensions of six adult specimens of an unidentified Pseudomys (Leggadina) species
(group 2), from SE. of the Blackstone Range, Central Western Australia, All females were lactating.
i
Y
9, M6344 | 9, M6345 | J, M6346 | 9, M6347 | 9, M6348 | 9, M6349
Wt. on capture (zm) 25 29 18 wu 29 214
Head and body (mm) &8 101) 380 83 \ 90 $1
Tail (mm) 59 62 58 59 69 56
Er (mm) 45 14 44 14 14 12
Hind-foot (mm) 17 17 16 16 18 16
ee a ood
* Pregnant.
TABLE 7
Skull dimensions of five adult female specimens of an unidentified Pseudamys ( Legquelina) species
(group 2) from SE. of the Blackstone Runges, Central Western Australia,
i
@, M6544 O, M6345 &, M6347 | 2, M6348 2, M6349
Greatest length 23-3 24-3 | 88-4 23:8 224
Basal length 10-9 212 21-1 20+3 19+2
Zygomatie hreadth 12-0 1304 12-2 12-5 119
Bruincase breadth Tet 1-7 11-0 11-0 10-8
Interorhitel Breadth 3-6 3:3 3+9 3-5 3:3
Nasals length ve) $3 7-9 8-0 7-9
Nasals breackth 2-2 2-4 22 2+4 2-3
Palatal length 12/0 12-8 12-0 12°35 11-5
Anterior palatal foramina Bel 5-4 5-1 H-1 4-7
Bulla 4:2 4-1 4-1 3-9 4:0
Upper molar series 4-7 4-8 465 4-4 4-4
Breadth of M1 1+6 1-6 16 1:5 1+5
J. A. Mahoney has examined a sample of the two preceding unidentified
groups, He placed both of them in the forresti-waitei-messuria group, and,
believing that its members are conspecific, tentatively called all our specimens
Pseudomys (Leggadina) forresti Thomas.
The relationships of what we have called Pseudomys {Leggadina) species
(group 1) and (group 2), and other native rodents will have to await further
collections, and study of new specimens and the types before any definile state-
ment can be made.
Pseudomys (Leggadina) hermannsburgensis Waite, sandy inland mouse.
(Plate 4, Figure 4)
Aboriginal Name: mingkiri — Pitjantjatjara, Nga:nyatjara (now used for all
small mice).
Localities. (i) 15 miles (24 km) E. of Mt. Ilbillee, Everard Ranges, NW.
South Australia; 132°43’E, 27°01’S; July 18, 1966; 3 ¢ and 3 ¢. (ii) Fregon,
NW. South Australia; 132°02’E, 26°47'S; July 16, 1966; 7 9 and 7a. (iti)
Bowden Hill, 80 miles (129 km) SW. of Mt. Woodroffe, Masgtave Ranges, NW.
South Australia; 130°41'E, 26°58’S; July 23, 1966; 1 29 and 1 @; 1 9 now
M 6354. (iv) Alkara, 90 miles (145 km) SW. of Mt, Woodroffe, Musgrave
Ranges, NW. South Australia; 190°30’E, 27°04’S; July 27, 1966; 3 ¢ and 3 3;
1 © now M 6353. (v) 42 miles (68 km) SW. of Mf. Aloysius, Blackstone Ranges,
Central Western Australia; 128°06’E, 26°25’S: November 12, 1966; 2 9; 1 3
now M 6355,
126 C. M. PHILPOTT ann D. R, SMYTH
Field Notes, This species was one of the commonest mammals between
128° and 132°F longitude and 26° to 27°S latitude. All specimens were taken
from burrows in sandy-loam soil, often in mulga (Acacia aneura) scrub, The
burrows were characterised by the absence of a large mound of soil neat the
mouth, as illustrated by Plate 4, Fig. 3. From one to four mice, with sex ratios
amongst them variable, were taken from single burrows. One female from
Fregon and two from locality (v) were pregnant, and a litter of four juveniles
was secn at Fregon,
The mean weight of 17 adult males which were weighed less than 24 hours
after capture was 11-1 + 0-4 gm with a range of 8 to 13 gm. For 9 adult, non-
pregnant females, the mean weight was 10-3 + I-4 gm, with a range of 9 to
13! em,
Taxonomy. Flesh and skull dimensions of the three specimens in the South
Australian Museum (M 6353-5) all fall within the limits given by Finlayson
(1841) for a large series of Ps, hermannsburgensis. Habits and coat wlour
which he described for this species are closely similar to those of our series,
Notomys cereinus (Gould), fawn hopping mouse,
(Plate 5, Figure 1)
Localities. (i) From 18 miles (29 km) S. to 70 miles (113 km) N, of Birds-
ville, SW. Queensland; 139°21'E, 25°54’S; fume 11-23, 1966; 3 ° and 7 @.
(ii) 5 miles (8 km) S. of Glengyle Homestead, SW, Queensland; 139°36’E,
Seine 9 8 and 9 &; 10 specimens from both localities now M 6357-65 and
M 6400,
Field Notes. This species was moderately plentiful, and all specimens were
taken while spotlighting at night on bare claypans and flats illustrated on Plate 1,
Fig. 2. It was seen on the same nights and in the same areas as Sminthopsis
crassicaudala and Antechinomys spenceri. All specimens were taken between
3 and 8 hours after sunset,
Taxonomy. ‘There was no gular pouch in any of the specimens but a marked
groove was present on the anterior surface of the upper incisors of 9 skulls
examined from individuals from both localities (M 6357-65). Finlayson (1959)
stated that these are characteristics of N. cervinus, and that they distinguish i
from N. fusciis (Wood-Jones ).
Notomys fuscus (Wood-Jones), Wood-Jones’ hopping mouse.
Locality. Pandie Pandie Homestead, Diamantina R,, NE. South Australia:
139°23'E, 26°07'S; summer of 1964-65; 1 ¢: M 6356.
—
Field Notes, This specimen was obtained by Mrs, L. Murton, who reported
thal similar hopping mice were often seen during the summer of 1964-65; we
found no live specimens while in the area.
Netomys alexis Thomas, northern hopping mouse,
(Plato 5, Figure 2)
Aboriginal Name: tarkawara—Pitjantjatjara, Nga:nyatjara.
Yocalities, (i) Turner’s Well, 22 miles (35 km) NE, of Mt. Woodroffe,
Musgrave Range. NW. South Australia; 132°00’F, 26°07'S: July 19, 29, 1966:
3 9.4 ¢ and 6J; 1 ¢ and 4] now M 6367, (ii) 14 miles (23 km) WSW. of
Mt. Aloysius, Blackstone Range, Central Western Australia; 128°21’E, 26°10°S
November 1, 1966; 2 9 and 15] (including 8 2 and 7 3 ); M 6369-85,
*
‘
SOME MAMMALS PROM INLAND AUSTRALIS iat
Field Notes, This species was common ever much of the area where we
found that Pseucdomys (Legeadina ) hermannsburgensis was plentiful. However,
we obtained roost N. alexis from more sandy areas, with less mulga serub. All
specimens were dug from burrows, From two to five juveniles were taken from
six single burrows; in four of these burrows lactating females were also taken.
The burrows had a vertical entrance shalt, about 6 to 18 inches (15 to 43 cm)
deep, and with na soil at the mouth. Horizontal “drives”, with occasional
branches extended from the base of the shaft to a maximum of about 6 feet
(1-8 m). At the end of the “drive”, a vertical escape shaft was often dug
stopping about an inch (2:5 em) below the surtace.
At levality (ii), empty shells of the quandong, Santelum acuminatum, were
found near the etitrance and along the “drive” vt oue N. alexis burrow, The
shells had bees opencd by removal of a small circular segment of the hard
outer coat.
DISCUSSION
Of the seven rare marsupials searched [or specifically, we located only
Macrotis lagotis, Because of the large fluctuations in numbers which o¢cur in
many desert-living species, and because we searched only a small proportion
of suitable habitats, it is by no means certain that any of the others are extinct.
However, only elderly aboriginal men had any knowledge of some of the species,
and this knowledge was obtained when they were young men, For example,
Myrmecobius fasciatus is spoken of as having gone for many years from the
Everard and Bedford Ranges. However, we should note that aboriginal people
everywhere are much less mobile aud dependent on vative mammals for food
now than they were: in Lhe past.
None of the 18 female Sminthopsis crassicaudata caught during June, July
and August had pouch-young though some of tle were toa young for breeding.
Conditions during this period were excellent, with recent rains having increased
plant and insect life. Martin (1965) recorded breeding of this species from
july to April under optimal conditions in the laboratory, It is therefore possible
that breeding in the wild is to some extent regular and seasonal, unlike the fairly
regular breeding noted under laboratory conditions,
Nearly all of the females of the unidentified Pseudomys (Psendomys)
species, Pseidomys (Leazgadine) species (group 1), and of Notomys alexis were
lactating, or were pregnant. Recent rains had resulted in good growth of herbs,
swhich had qwaltured and shed their seed,
This large-scale, synchronous breeding of native rodents and consequent
population increase. can perhaps explain to some extent the taxanomic difficiilty
ot this group, ‘That there are large fluctuations in numbers of many native
rodents has often been noted, especially m arid regions such as the Lake Eyre
Basin (e.g, Finlayson, 1939a). A large increase in variability has been observed
wher a large increase in the numbers of several animals has occurred. Ford
and ford (1930), working with the butterfly Melitaca aurinia, were one uf the
first to draw attention to this lurge increase in variability. The presence of much
variation in rapidly increasing populations of rodents would tend to decrease
the number of differential characters which could be used to separate closely
related species. Also, variability of the one species from different areas would
probably be large. This is because populations from different localities would
perhaps be derived from isolated small numbers of individuals present before
the large increase.
128 C. M, PHILPOTT axn TD. KH. SMYTIT
Finlayson (1961) considered that pastoral exploitation, and the introduced
rabbit, fox and domestic cat were important factors influencing the abundance
and range of Central Australian species. In order to conserve at least some of
these species, they must first be located. Then, the influence of the above factors
should be analysed. Finally, suitable areas should be proclaimed as reserves, and
some contrel of the environment attempted in order to minimise these deleterious
factors. We hope our study has contributed ta the first step in such a programme
ol urgent conseryation,
ACKNOWLEDGMENTS
This study was carried out as part of the scientific work of the Royal Zoo-
logical Society of South Australia Inc. and was made possible by a generous grant
from the Nuffield Foundation te Dr. P. S. Watts, its president.
We are extremely grateful to Professor H. G. Andrewartha, of the Depart-
ment of Zoology, University of Adclaide, for many discussions and useful guicd-
auce throughout the year, We also thank Dr. S. Barker for much encouragement
and interest. The Council and staff of the Royal Zoological Society of South
Australia, and especially Dr. P. S, Watts and Mr. W. E, Lancestcr, made our task
lighter with unlimited help. We received much help and cooperation from the
various State Fauna Authorities, and especially the South Australian Department
of Fisheries and Fauna Conservation. We are appreciative of help and under-
standing fram the South Australian Department of Ahoriginal Affairs and the
West Australian Department of Native Welfare. The South Australian Museum
provided us with unlimited facilities for which we are most thankful.
In the field, we received nothing but kind hospitality and cooperation from
many station residents. Dr. and Mrs, G, C. Gregory of Leigh Creek township
were especially helpful, The staff at Fregon, Ernabella, Musgrave Park an
Warburton Ranges made our stay in their area both fruitful and enjoyable,
Finally, we have spectal thanks for Mr. T. Dodd, and those people from the
Pitjantjatjara and Nya:nyatjara tribes whose help was entirely insttumental in
dur success while working in their lands.
REFERENCES
Cimon: H., 1963. Australia’s Threatened Mammals. Wildlife, Brisbane, 1; No, 1, pp,
5-18,
Deveias, W. H., 1984, An Introduction to the Western Desert Lapguage, Oceania Lin
guistic Monogr, No, 4 (revised). (University of Sydney: Sydney, }
Wriayson, H, H., 1939a. On Mammals from the Lake Eyre Basin: Part V. General Re-
marks on the Increase of Murids and their Population Movements in the Lake Eyre
Basin during the Years 1930-36. Trans. R. Soc. 8, Aust., 63, pp. 348-3473_
Myiarson, H. H.. 1938h. Records and Descriptions of Muridae from Onldea, South Ans
tralia. Trans. H. Soc, 5. Aust. 63, pp. 354-364.
Frt.ayson, H. H,, 1941, On Central Australian Mamynals; Part H, The Muvidae (con-
tinued). ‘Trans, R. Soc. S$. Aust., 65, pp. 215-232,
Fuxtayson, HW. H., 1960. Nomenclature of Notomys (Muridae) jn the Lake Eyre Basil,
Trans, R. Soe. $. Aust., 83, pp, 79-82,
Foxcayson, HW. 11, 1961, On Central Australian Mamunals: Part IV, The Distribution and
Status of Central Anstralion Species. Rec, S. Aust. Mus., 14, pp, 141-191,
Fouv, H. D., and Forn, E. B., 1930. Fluctuation in Numbers, and its Influence an Variation,
in Melitaea aurinia, Rott, (Lepidoptera). Trans. R. ent. Sac, Lond., 78, pp, 345-952.
Mack, G,, 1961. Mamuials from South-western Queensland. Mem, Od. Mus., 15, pp,
215-229.
SOME MAMMALS FROM INLAND AUSTRALIA 129
Martin, P. G., 1965. The Potentialities of the Fat-tailed Marsupial Mouse, Sminthopsis
crassicaudata (Gould), as a Laboratory Animal. Aust. J. Zool., 13, pp. 559-562.
Tate, G. H. A., 1951. The Rodents of Australia and New Guinea. Bull. Amer. Mus. nat.
Hist., 97, pp. 183-430.
Tuomas, O., 1910. The Generic Arrangement of the Australian Murines Hitherto Referred
to as Mus. Ann. Mag. nat. Hist., 8, pp. 603-607.
Troucuton, E., 1932. On Five New Rats of the Genus Pseudomys. Rec. Aust. Mus., 18,
pp. 287-294.
Troucuton, E., 1964. A Review of the Marsupial Genus Sminthopsis (Phascogalinae), and
Diagnoses of New Forms. Proc. Linn. Soc. N.S.W., 89, pp. 307-321.
Woop-Jonges, F., 1923-5. “The Mammals of South Australia, Parts I, II and III.” (Govern-
ment Printer: Adelaide. )
C. M. Puiteorr ann D. R. Smyrin PLATE 1
Fig. 1. Male Sminthopsis crassicaudata from near Birdsville, approx. life-size.
Fig. 2. Looking along a stabilized sand-ridge 3 miles east of Birdsville where we caught 6
S. crassicaudata. Notomys cervinus was also living nearby.
Fig. 3. Tracks of a captive male S. crassicaudata from Glengyle. Direction of travel is from
bottom to top, and the scale is in inches and centimetres (see text).
C. M. Puteeotr ANp D, R. SMyTH PLATE 23
Fig. 1. Immature female rabbit bandicoot (Macrotis lagotis) from south of the Blackstone
Ranges, approx. 4 life-size,
Fig. 2, A male black-flanked rock wallaby (Petrogale lateralis) taken in the wild at Alkara.
south of the Musgrave Ranges,
Fig. 3. Alkara, 90 miles south-west of Mt. Woodroffe. We observed P. lateralis on the
darker rock on the left of the hill. We caught Pseudomys hermannsburgensis on the
sand ridge in the foreground,
C. M. Puitpotr ann D. R. SaiviTn PLATE 3
Fig. 1. An adult female Psendomys (Ps.) minnie or rawlinnae, obtained as a juvenile from
Wire Creek Bore, approx. 0-65 x life-size. Each division of the scale is 1 centimetre.
Fig, 2. Habitat at Wire Creek Bore 20 miles north of Oodnadatta. The shrub in the fore-
ground is the silver saltbush, Afriplex rhagodioides. On this plain we caught
Sminthopsis crassicaudata, 8. larapinta, Ps. minnie or rawlinnae, and an unidentified
species of Ps, (sub-genus Leggadina).
Fig. 3. A burrow of Ps. minnie or rawlinnae under a silyer saltbush at Wire Creek Bore.
The mound at the entrance is approx. 9 inches wide.
|. M. Parueorr Ann D. R. Smyrin PLATE 4
Fig. 1. An unidentified male Pseudomys (Leggadina) species from 30 miles north of Birds-
ville, approx, 0-6 x life-size,
Vig. 2. Tracks of the Ps. (Leggadina) species shown in Fig. 1. Direction of travel is from
bottom to top, and the scale is in inches and centimetres (see text).
fig. 3. Entrance to a Pseudomys hermannsburgensis burrow near Fregon.
Fig. 4. A male Pseudomys (Leggadina) hermannsburgensis from Alkara, south of the
Musgrave Ranges.
C. M. Puitporr Anp D, R. SmyrH PLATE 5
Fig, 1. A male Notomys cervinus from near Birdsville, approx. 0-6 x life-size.
Fig, 2. A male Notomys alexis from Turners Well, near Ernabella, approx. 0-6 x life-size.
Fig. 3. Habitat of an unidentified Ps. (Leggadina) species (group 2). 20 miles south-
south-east of Mt. Aloysius.
Fig, 4. Entrance to a burrow of Ps. (Leggadina) species (group 2), at the locality shown
in Fig. 6, The burrow contained an adult male.
FOSSIL ELASMOBRANCH TEETH OF SOUTH AUSTRALIA AND THEIR
STRATIGRAPHIC DISTRIBUTION
BY N. S. PLEDGE*
Summary
Several hundred fossil elasmobranch teeth, collected from Tertiary formations in South Australia,
have been identified to species level in most cases. Twenty-five species have been recognized,
including the new species Carcharias maslinensis Pledge, and three forms are identifiable only to
genus level. The majority of species belong in the Infra-class Osteodonta, and some absentees are
noted. Diagnoses for the various genera and species are given, and a guide to their salient features.
When the occurrences are arranged stratigraphically, they fall into two main time spans, in
Middle to Upper Eocene and Lower to Middle Miocene, when conditions were most suitable for
preservation. It is concluded that the establishment of zones in Australia, based on assemblages of
elasmobranch teeth, is not yet possible.
FOSSIL ELASMOBRANCH TEETH OF SOUTH AUSTRALIA AND
THEIR STRATIGRAPHIC DISTRIBUTION
by N. S. Prepc*
[Read 14 September 1967]
SUMMARY
Several hundred fossil elasmobranch teeth. collected from Tertiary forma-
tions in South Australia. have been identified to species Jevel in most cases.
Twenty-five species have been recognized, inchiding the new species Carcharias
maslinensis Pledge, and three forms are identifiable only to genus leyel, The
majority of species belong in the Infra-class Osteodonta, and some absentecs
are noted, Diagnoses for the various genera and species are given and a guide
to their salient features. When the ocettrences are arranged stratigraphically.
they fall into two main time spans, in Middle to Upper Focene and Lower to
Middle Miocene, when conditions were most suitable for preservation. It is
concluded that the establishment of zones in Australia, based on assemblages
of elasmobranch teeth, is not yet possible.
INTRODUCTION
The Elasmobranchii have a history reaching back to the Devonian Period,
but many major groups became extinct before or during the Mesozoic, Although
marine sequences of Cretaceous age are known in South Australia, no shark
remains have been recorded from them yet. All the teeth described herein are
from Tertiary deposits.
Apart from a brief note by McCoy (1875), Chapman (1913, 1914, 1917),
Chapman and Pritchard (1904, 1907), and Chapman and Cudmore (1924)
have been the only ones to write on the Tertiary fishes of Australia, Most of
their material was from Victoria; only rarely were South Australian specimens
mentioned.
The first work of any importance concerning fossil fishes was by Louis
Agassiz, whose “Recherches sur les Poissons fossiles” was published at Nen-
chatel between 18384 and 1843. Other papers soon followed in Europe and
America, and a few workers studied the fossil fishes of Indo-Pacific region. Very
recently, L, S$. Glikman (1964), of the Academy of Science of the U.S.S.R.,
published a volume wherein assemblages of sharks’ teeth are used to define
twelve zones in the Russian Paleogene, The present work was undettaken to
determine whether similar zones could be established for the Australian
Tertiaries.
MATERIAL
The paleontological collection of the Department of Geology, University of
Adelaide, includes several hundred fossil elasmobranch teeth, mostly from local
Tertiary formations. A large number of teeth in the collection of the Geological
auvey, of South Australia, and several small private collections, were also
studied.
* University of Adelaide. Present address: Geolugy Dept., University of Wyoming, U.S.A.
Trans. Roy, Soc, S. Aust. (1967), Vol. 91.
16 \. 8, PLEDGE
DEPOSITORIES
Teeth held in the Department of Geology, University of Adclaide, ave
catalogued with the prefix “i”.
Those in the collection of the Geological Survey are recorded in the Verte-
brate Catalogue, and have timbers with the prefix “V", e.g, V35.
NOMENCLATURE
Many elasmobranch genus names were established by naturalists of the
eatly 19th century, such as Rafinesque (1810), de Blainville (1816) and Cuvier
(1817). Cuvier is best known, but many of the genera he established were
synonyms. Agassiz propagated these synonyms in the literature, and it is only
in yecent years that the original names have come into more general usage for
the fossil species. Some authors, such as Glikman (1964), have split these
“classical” genera, but it is difficult to see their reasons for so doing,
As genera and species of fossil sharks are established only on the character
of the teeth, it is obvious that both “splitting” and “lumping” may occur. Com-
parison with the teeth nf living sharks can reduce this risk somewhat, according
lo the particular genus of shark, but not remove it, Many species are therefore
only morpho-species, and may represent several different biospecies, or con-
versely one biospecies may be represented by several morpho-species. As far as
possible, the teeth described herein are compared with species originally de-
scribed from Europe or America, on the grounds that most species of larger
sharks have very wide distributions, and the number of parameters by which
sharks’ teeth are identified are not sufficient to establish geographic species for
similar forms from different parts of the world.
CLASSIFICATION
Several classifications of sharks have been proposed and these vary widely.
Most have a strictly zoological approach, using characters, rarely, if ever, pre-
served in fossils. Nicholson and I,ydekker (1889) used a major division based
on the structure of the vertebrae, Tectospondyli and Asterospondyli, while
Bertin and Arambourg (1958) had major Aivisions, Pleurotremata and Eypo-
tremata, based on gill position, i¢. more or less on body form. Smaller divisions
ate based on morphological and physiological eriteria in which tooth form is
rarely included. Families and orders of fossil sharks’ teeth are therefore hased
on living forms. However, the major division in fossil sharks is one of the basic
tooth: structure, and this has been utilised by Glikman (1964) in his classifica-
tion of extinct and living clasmohranchs, which is marked by a distinction
hetween orthodont and osteodont dentition.
Orthodont teeth (Text-fig. la) have a pulp cavity surrounded by artho-
dentine, and such teeth are found in the majority of living and fossil elasmo-
branchs, including one order of “true” sharks, the Carcharhinidae (whalers,
topes, tigers and Fathmerhead sharks}, also the dugfishes, rays and skates, and
those primitive sharks: the hexunchids (notidanids) and heterodontids.
The Osteodonta have teeth (Test-fig. Ib) whose compasition, including
the root, is a vascular bone-like form of apatite called osteodentine. Only “trac”
sharks are included in the group: nurse and sand sharks, bulldog sharks, por-
heagles, makos and blue pointers, threshers, and white pointers.
This division raises the question: which feature is of greater phylogenetic
importance — a basic tooth structure, a basic vertebral structure, ar overall hedy
shape and anatomical layout?
FOSSIL ELASMOBRANCH TEETH OF S.A. 137
sary AAD)
Fig. 1. a. Orthodont tooth (Carcharhinus), b. Osteodont tooth (Carcharias), e; Fnamel
(vitrodentine), or: orthodentine, os: osteodentine, ps: pseudodentine, p: pulp cavity
(diagrammatic sections, after Bertin and Arambourg, 1958).
Fig. 2. a. Profile, Carcharias macrotus. b. Inner face, ditto. c. Lamna_apiculata, inner face.
d: lateral denticles, e: entire margin, 1: root lobe. m: median boss, n: nutritive pit,
§: striations.
Fig. 3. a. Serrated margins, e.g. Galeoverdo. bb, Serrated margins, e.g. Hemipristis, c, Den-
tate marftins, e.g. Carcharodon,
Fig. 4. Carcharias arenarius Ogilby. a. Upper jaw. b. Lower jaw. Anterior at left,
ot
Fig. 5. Istiropsis mako (Whitley). a. Upper jaw. b. Lower jaw. Anterior at right.
TAs N. §, PLEDGE
However, the tossil record furnishes mainly the teeth, and the vertebrae
found are difficult to ascribe to families. The use of the divisions Tectospondyli
aod Asterospondyli has been generally discontinued, and it is therefore felt
that the use of basic tooth structure as a criterion for classification is defensible.
TOOTH MORPHOLOGY AND VARIABILITY
(‘Text-figs. 1-5)
Sharks’ teeth consist of two main parts —the crows or biting, surface, and
the root. The crown inay be solid (ie. osteodont) or hollow (orthodont),
The crown consists of the main cusp or cutting blade, which may possess
some accessory cusps, In osteodont sharks, these are paired lateral denticles or
cusps; but in some orthodont sharks the tecth are asymmetrical, and accessory
cusps Occur only or mainly one the posterior side, e.g. “Notidanus” and Geleo-
cerdo. The crown is often compressed into a blade, with the labial (outer)
face being more planar than the lingual (inner) Face.
The margins may be sharp cutting edges or quite blunt. Unless they are
interrupted by dentes or serrae, they are termed “entire”. Dentes are squarish
“teeth” produced by invaginations of the edge, and serrae are saw-like points;
intermediate shapes also occur,
Paired Jateral denticles may take a variety of forms, even within the one
species: sharp-pointed cones or barely discernible tubercles, straight or curved,
broad sharp-edged compressed cones, or wedge-shaped blades. They may also
bewr serrac or dentes.
Ornamentation of the enamel is often present: plications of the enamel of
the outer face, and longitudinal striations on the inner face.
The root is of bone-like material. and is usually bifurcated into two more
or less distinct lobes which can take a variely of forms, according to position in
the jaw. At the middle of the inter side of the root there is often a “median
boss" which bears a yertical groove containing the “nutritive foramen”. This
is inainly seen in osteodont teeth, but some carcharhinids also have a nutritive
pere. Within any one species of shark, variation in tooth form is seen; it may
be slight, involving only an increasing obliquity in tha more distal teeth, or
radical. as in the hexanchids, where the difference between teeth of upper and
lower jaws is extreme. Some generalisations may be made, although exceptions
can be found.
i. Tecth from the upper jaw are broader than their lower jaw equivalents.
2. Upper tceth show more inclination than the equivalent lower tecth,
which are normally erect.
3. ‘There is a gradual decrease in the lungth-breadth ratio of the crowns
as one proceeds backwards in the jaw.
4. Tn sharks having “eye” teeth (which are considerably smaller than their
immediate neighbours), the anterior teeth are considerably more elongate
than those lateral teeth immediately followmg the eye teeth,
There may be an increase in the number of latcral cusps on teeth in the
distal parts of the jaws; the cusps also become broader and relatively
coursér.
6. Small symphysial teeth may occur at the symphysis of either jaw,
The living sharks, Carcharias arenarius and Isuropsiy mako ( Text-figs. 4, 5),
found in South Australian waters, show many of these features, Others, such as
Galeocerdo and Carcharadon, show little variation within the jaw, save inelina-
tion and crown proportions.
a)
FOSSIL ELASMOBRANCHL TEETH OF S.A. 189
Measurements are taken along three approximately perpendicular directions.
Generally, crown height only can be measured due to damage to the root, and
this is taken in the plane of the outer face, from apex to base, in a line per-
pendicular to the base. Width is measured at the base of the crown, where it
naturally scparates from the root, Thickness is often difficult to measure be-
cause of the configuration of the tooth; it is taken in a line normal to the outer
face, as close to the base as possible.
TAXONOMIC CHARACTERS
The characters that define genera of sharks’ teeth are in some respects quite
vague, yet in conjunction they serve to separate the groups fairly well.
Features used are:
Overall shape and proportions.
Presence or absence of serrated margins,
Presence or absence of latera! cusps.
Shape and number of lateral cusps, if present.
Shape of the roots.
Specific characters are the same as those listed above, with the addition of:
6. Presence or absence of striations on the lingual face.
7. Presence or absence of plicae in the enamel of the labial face.
8. Contortion or inclination of the crown.
In addition to just the presence or absence of these features, specific deter-
minations also depend considerably on the degree to which a character is pre-
sent. This can, and undoubtedly does, lead to some confusion in identification
from inadequately illustrated descriptions,
SYSTEMATICS
The classification used herein is given below, and is adapted from those
of Glikman (1964) and Bertin and Arambourg (1938),
Superclass Pisces
Class Chondrichthyces
Subclass Elasmobranchii
Infraclass Orthodonta
Order Hexanchida
Family “Notidanidae” (Hexanchidae)
Order Heterodontida
Family Heterodontidae
Order Squatinida
Suborder Rajoidei
Families including Pristidae, Rajidae, Myliobatidac, Dasyatidae
Suborder Squatinoidei
Pristiophoroidei
Orectoloboidei
Squaloidei
Order Carcharhinida
Family Carcharhinidae
Sphyrnidae
Infraclass Ostcodonta
Order Carchariida
Family Carchariidae (= Odontaspidae)
Isuridae
GU GA po po
140 N, $5. PLEDGE
DESCRIPTION OF SPECIES
Infraclass Orthodonta
Family “Notidanidae”
Genus “Norwanus” Cuyier, 1817
Diagnosis. Teeth of upper jaw with prominent prime cusp and one or more
small secondary cusps on distal side. Lower teeth very wide with numerous
secondary cusps giving a saw-like form.
“Notidanus” Cuvier includes Iexanchus and Heptranchias Rafinesque,
1810, and Notorhynchus Ayres, 1855, as there is no apparent generic difference
between the teeth of these living genera.
“Notidanus” serratissimus. Agassiz
(Plate 1, Figs. 1-3)
Notidanus serratissimus Agassiz, 1843, p, 222, pl. 36, figs. 4, 5,
Woodward, 1886, p. 216, pl. 6, figs, 23-26,
Diagnosis, Teeth small, five to ten cones with blunt apices; principal cone
ouly slightly larger than immediate neighbour, but more robust. Anterior edge
produced downwards and denticulated on lower half.
Observations. Woodward's figures 24 and 25 (1886) most closely agree
with two teeth at hand, although one of these has eleven cones—more than pre-
scribed by the diagnosis. In all other respects, including gcologic age, they
agree with the figured material.
Another specimen, however, from the Naracoorte Bore, exhibits a somewhat
different form. The principal cusp is very broad and less acute, and about
twice as high as the following cusps which are about the same height. It also
has eleven cusps.
Four fragments (Pl. 1, Fig, 3) found in close proximity at Blanche Point
are tentatively assigned to this species, although they show some variation in
the coarseness and style of serration.
Occurrence. Blanche Point Marl, at Port Noarlunga and Blanche Point.
Knight Formation equivalents, Naracoorte Bore, 426 ft.
Age. Middle and Upper Eocene.
Material Examined. ‘Three teeth and several fragments.
Family PRISTIDAE
Genus Pristrs Latham, 1794
Diagnosis. Rostrum of skull long smooth blade with rounded end and
parallel sides. Rostral teeth triangular, compressed dorsoventrally, faintly
striated lengthwise, occur regularly along rostrum.
Pristis cudmorei Chapman
(Plate 1, Fig. 6)
Pristis cudmorei Chapmun, 1917, p. 139, pl. 9, fig. 7.
Diagnosis. Rostral teeth small, elongate, triangular, slightly inclined. An-
terior margin sharp, finely denticulated to apex. Posterior edge thick and blunt,
Both faces yery finely and irregularly striated for half of height.
FOSSIL ELASMOBRANCEHE TEETH OF 5.A,. 141
Observations. ‘The three specimens at hand agree closely with Chapman's
description of material of Upper Miocene age, but full equivalence of this
neritic form is doubted because of the large time gap between the Victorian and
South Australian occurrences.
Occurrence, Blanche Point Marl, Maslin Bay.
Age, Upper Eocene. Carter's Unit 2.
Material Examined. Three specimens.
Family MYLIOBATIDAE
Genus Mytiopatis Cuvier, 1817
Diagnosis. Dental pavement formed by regular interlocking of hexagonal
tooth plates. Tooth plates with comb-like base—numerous transverse parallel
blades on articulating surface. Median plates very broad, lateral plates regular
hexagons.
Myliobatis spp.
(Plate 1, Figs, 4, 5)
Observations. Two pieces from the Blanche Point Marl, and six pieces of
different species from Naracoorte are the only South Australian specimens seen
by the author. A fragment of caudal spine (PI. 1, fig. 5) is also referred to
this genus, but none of the material has been identified to species level.
Qceurrence. Blanche Point Marl, Maslin Bay; Naracoorte E, & WS. Bore
No. 5, 426 ft., Knight Group equivalents,
Age. Middle and Upper Eocene.
Material Examined. Spine fragment from Blanche Point, 6 tooth plate
fragments from Naracoorte bore, 2 from Blanche Point.
Family CARCHARHINIDAE
Genus Cancearuinus Blainville, 1816
Diagnosis. Teeth small, stout; lower teeth narrow, erect; upper teeth
broader, inclined. No lateral denticles. Base widely expanded, Cutting margins
often finely serrated. Root nearly straight, with central notch,
Carcharhinus of. collatus Eastman, 1904
(Plate 1, Fig, 7)
Carcharias collata Eastman, 1904, p. 85, pl 32, fig. 3.
Chapman and Cudmore, 1924, p. 118, pl. 9, figs, 13-16,
Diagnosis. Robust Carcharhinus teeth with cutting edges finely serrated
on basal prolongations, very finely on cusp, entire apex, Inner face strongly
convex, Enamel of outer face extends much Jower than on inner face. Root
elongated, large, symmetrical,
Observations. The four specimens at hand agree with the figure of C,
collatus given by Chapman and Cudmore (1924), and also with Eastman’s
figures of his types from the Miocene deposits in Chesapeake Bay, Maryland,
although one specimen is more oblique, and another more robust.
Occurrence. The teeth all came from 255 ft, depth in the Marion No. 2
Bore, Sturt River Valley, Adelaide Plains, ‘This depth is in or near the Munno
Para Clay member of the Port Willunga Beds, as defined by Lindsay and
Shepherd (1966).
Age. Lower to Middle Miocene: Batesfordian-Balcombian.
Material Examined. Four specimens,
142 N. 8, PLEDGE
Carcharhinus (Prionodon) aculeatus (Davis)
(Plate 1, Fig. 8)
Caleocerdo aculeatus Davis, 1888, p, 8, pl. 1, figs. 1-3,
Carcharias (Prionodon) ucyleatus Woodward, 1889. p. 440.
Chapman and Cudmore, 1924, p. 119, pl. 9, figs. 19, 20.
Diagnosis. Carcharhinus teeth with whole cutting margin serrated, rather
coarsely on lateral prolongations, finely on cusp, coarsest in notch; apex almost
entire.
Observations, This species is represented by a solitary tooth from the River
Murray Cliffs. It is similar to specimens of C. collatus at hand, but the serra-
tions are considerably coarser and the tooth is slightly larger. The cusp shows
a distinct inclination and the anterior notch is shallow. “The tooth compares
favourably with the figures of Chapman and Cudmore (1924).
Oceurrence. River Murray Cliffs, locality uncertain, preseryation suggests
Cadell Marl Lens, Davis’ material came from the Oamaru area (?L. Miocene)
and from the L. Pliocene “Awatere Series”.
Age. Lower Miocene.
Material Examined. One specimen,
Wet: wel ‘
Genus Hemurrusris Agassiz, 1843
Diagnosis, Principal tecth large, triangular, compressed; cutting edges
coarsely serrated almost to apex. Lower anterior teeth slender, subulate, in-
wardly curved, only a few minute serrae at base.
Hemipristis serra Agassiz
(Plate 1, Fig. 9)
Hemipristis serra Agassiz. 1843, p. 237, pl. 27, figs, 18-30.
Woodward, 1889, p, 449,
Chapman and Cudmore. 1924, p, £15, pl. 9, fig: 12.
Diagnosis, Marginal serrations in broad upper teeth large, extending
almost to apex. Margins of anterior lower teeth very sharp distally, Toner
face of root with deeply cleft median boss.
Observations. This species, while couimon in the Tertiaries of Europe,
America and Indonesia, is quite rare in Australia, and only twe specimens are
known to the author, one found by Cudmore (Chapman and Cudmore, 1924)
and the other very recently by Mr. R. J. F. Jenkins. The latter specimen is
slightly smaller, but broader than that figured by Chapman and Cudmore. The
marginal serrations are coarse, very sharp, and stop about 5 mm below the apex.
The crown is inflated, but the external face is depressed at the base; the margins
are twisted, convex outwards. Most of the root is missing.
Occurrence, Cliff, left bank of River Murray, one mile below Pelican
Point, near Morgan, South Australia. Cadell Mar] Lens in the Morgan Lime-
stone,
Age. Lower Miocene - Batesfordian,
Material Examined, One specimen (F17288).
Genus CarcHarowres Ameghino, 1901
Diagnosis. Teeth similar to Lamna, but with denticulated margin as in
Carcharodon. Lateral denticles compressed, dentate. Orthodont.
FOSSIL ELASMOBRANCH TEETH OF S.A, 143
Carcharoides cf. totuserratus: Ameghino
(Plate 1, Fig, 11)
Carcharnides tatuserratus Ameghino, 1906, p. 183 (footnote), fig. 50.
Chapman and Cudmore, 1924, p. 121.
Diagnosis. Teeth large; inclined crowns. Large pointed lateral cusps, all
margins denticulated.,
Description of Specimen. Crown elongate triangular, acute, slightly oblique.
Margin irregularly dentate, dentes wide and separated by shallow grooves,
Outer faec almost Hat, smooth, inner face convex, smooth,
Observations. The sole specimen at hand consists only of the enamel shell
of the crown, and no root or lateral denticles are present. It is somewhat
smaller than Ameghino's type, and less oblique, and shows a flaring of the base
that is difficult to visualize in C. totuserratus, It is also similar to C. tenuidens
Chapman; Chapman records both forms from Janjukian deposits at Waurn
Ponds, Victoria; Ameghino's material, from the Patagonian Series, is now re-
garded as being of Lower Miocene age.
Oceurrence. Road cutting near Strathalbyn cemetery, Mannum Formation
equivalents.
Age. Lower Miocene.
Material Examined. One specimen.
Genus Gateocerpo Miiller and Henle, 1838
Diagnosis. Teeth serrated on both edges. Apex sharply inclined, deep
notch posteriorly, coarse serrations below notch,
Galeocerdo cf. aduncus Agassiz
(Plate 1, Fig. 10)
Galeacerda aduneus Agassiz, 1843, p. 231, pl. 26, figs. 24-28,
Woodward, 1889, p. 444,
Chapman and Gudmnore: 1924, p. 117.
Leriche, 1957, p, 38, pl. 45, figs, 18-21,
Diagnosis. Anterior margin arched; apex short, broad, sharply inclined,
very similar to existing Galeocerdo cuviert but smaller,
Observations. There is only one South Australian specimen of this species
at hand. At first glance it seems referable to G. lutiélens because of its rela-
tively great width and low crown. However, the anterior margin is distinctly
arched, and finely denticulate. On reference to a jaw of the living G. cuviert,
it would appear that the tooth came from a posterior position, where the crown
is relatively low.
Another tooth (Plate 1, Fig. 10b), of presumed Miocene age, and from
an uncertain locality, is at hand. It differs from the above in having an elon-
gated apex reaching almost to the posterior extremity of the tooth. The anterior
edwe shows a sharp bend about halfway along its length, and the two halves
are straight. As such, it does not fit any species known to the author, but no
attempt has been made to erect a new species on it at this stage.
Occurrence. Exact locality unknown, but from the River Murray cliffs,
probably at Morgan.
Age. Lower Miocene.
Material. Examined. Two teeth.
144 N, 5. PLEDGE
Family TRIAKIDAE
Genus Musterus Linck, 1790
Diagnosis, Tecth small, similar, rhomboidal occlusal surface, arranged in
oblique rows to form wide curved dental pavement on jaws; many in function
at same time:
Fig. 6
Fig. 6. Comparison of Mustelus antarcticus and PMustelus sp,
. M. antarcticus, occlusal surface, Recent.
. PMustelus sp., ditto (17287), U, Eocene.
M. antarcticus, postero-occlusa) aspect showing length,
. PMustelus sp., ditto. (x 5 approx.)
a
ec
b
d
cf, Mustelus sp.
(Text-fig, 6)
Description. A single, small, subrhomboidal tooth was found by Mr. R. J, F.
Jenkins at Blanche Point, It is similar in form to a tooth from the living gummy
shark Mustelus antarcticus Gunther, but differs in that the posterior corner of
the rhomb is truncated, while the anterior truncation is wider.
The gently arched occlusal surface of the tooth is granulate, but there is
a distinct smooth triangular area at the posterior corner (in the living M, antarc-
ticus the whole surface is granulate, more coarsely on the posterior half). The
tooth is not as deep as M; antarcticus, and its articulating process is obscured or
missing.
Observations. This is the first report of any tooth of this form from Aus-
tralian Tertiaries, although the Triakidae have a history reaching back to the
Cretaceous, and Mustelus itself has been recorded from Oligocene deposits
(Arambourg and Bertin, 1958, p. 2036).
If the present determination is correct, the genus will thus have its strati-
graphic range extended back to the Upper Eocene.
Occurrence. Blanche Point Marl, Maslin Bay.
Age. Upper Eocene, Aldingan Stage, Carter’s Unit 2.
Muterial Examined. Oue specimen, plus example from hving gummy shark.
Infraclass OsrEoponTA
Family CARCHARIIDAE (= ODONTASPIDAE)
Genus CarcHanAs Rafinesque, 1810
(syn. Opontasris Agassiz, 1843)
Diagnosis. Teeth with high, narrow, compressed crown; with one or two
pairs of lateral denticles, generally sharp pointed. Anterior teeth very high
crowned, large and slender, with much produced bifurcated root. Similar to
Cretaceous Scapanorhynchus and some forms of Lamna, Cutting edges entire,
beginning several millimetres above base of crown,
FOSSIL ELASMOBRANCH TEETH OF S,A, 143
Carcharias macrotus (Agassiz)
(Plate 3, Figs. 1-8)
Lemna eleguns Agassiz, 1843, p. 289, pl. 35, figs. 1-7, pl 37a, figs. 48, 59.
Otedus macrotus Agassiz, 1843, p. 273, pl. 32. figs. 29-81
Odontaspis elegans Woodward, 1889, p, 361.
Q. macrota Woodward, 1899, p. 9. pl. 1, figs. 19, 29,
O. mactota striata White, 1931, p, 58, figs. 45-74.
Diagnosis. High narrow crown, slightly curved; outer face smooth,
slightly convex; inner face convex but medially flattened, longitudinally striated,
striae rather irregular, Single pair of lateral denticles. Prominent median hoss
with nutritive pore. Root lobes long, generally pointed.
Observations. Teeth of this species show a variety of forms, depending on
position in the jaw, and also, to some extent, on age. The denticles show a
number of different forms, from fine curved cones to broad compressed cones,
to chisel-like blades. Striations vary in continuity und degree, from strongly
incised groves to barely discernible narrow facets. Many specimens lack the
root and/or lateral cusps, making identification rather uncertain. Several bio-
species may be represented. According to White (1931, p. 62) the forms
“Odontapsis elegans” (Ag) and O, macrota are the same species, “O, elegans”
being juvenile to O, macrota.
Two other forms have heen separated in the South Australian material. One
is represented by six teeth (V49) from the Naracoorte bore assemblage (Plate
3, Fig. 7), They differ from most specimens in having a quite robust habit
with short narrow crowns and strong, thick, widely bifurcated rocts, AI show
the typical C, macrotus striations. Three of them are from the upper jaw,
having shorter, inclined crowns. All bear short lateral cusps, and fwo of the
lower teeth also have a second, minute, inner pair-
The other aberrant form (Plate 3, Fig. §) is represented by three teeth
{V53) from the Pecl’s Bore assemblage, which differ in size. preservation and
roat form from the numerous specimens of C. macrotus also present. Al! three
bear strong striations, and lack lateral cusps, One is a compressed symphysial
tooth, and the other two have roots with widely divergent, Hattened, round-
ended lobes,
Not enough is known of these two forms ta put them in other specics.
Occurrence, Basal member of the Tortachilla Limestone, upwards ta the
lower part of the Port Willunga Beds—Maslin and Aldinga Bays. Peel’s Bore
near Robe (390 ft.), and an aberrant form from the E. & W.S. Bore No. 3, at
Naracoorte (426 ft.). Alsa from fhe Strathalbyn cemetery road cutting, Morgan
type section, and Dry Creek Sands (Tenant's Bore, Salisbury).
Age. Common in Middle and Upper Eocene, and sporadically to Pliocene,
in South Australia,
Material Examined. Approximately 50 specimens from Maslin and Aldinga
Bays in A.U, catalogue; about 100 from Peel's Bore and otber places, held in
the Geological Survey collection, including the aberrant forms (V49 and 53).
Carcharias contortidens (Agassiz)
(Plate 3, Fig, 1L)
Lamna (Odontaspis) contartidens Agassiz, 1843, p. 294, pl. 37a, figs. 17-23,
Qdontuspis contortidens Woodward, 1889, p, 366,
Chapman and Cudmore, 1924, p. 122.
Diagnosis, Teeth slender; delicate longitudinal striae on inner face, Sig-
moidal curvature of anterior teeth and median boss of root more pronaunced
than in C. macrotus.
lt N. S, PLEDGE
Observations. A large number of teeth from Peel's Bore were separated
from C. macrotus hy their greater slenderness and sinuosity, The striations are
often finer and more uumerons than in C. macrotns and extend nearer to the
apex, Miocene specimens from the Marion No. 2 Bore are similar to, but
cousiderably smaller than those from Peel’s Bore.
Occurrence. Peels Bore (390 ft,), near Robe; Mario No. 2 Bore (255 £t.),
Sturt River Valley; Blanche Point Marl, Aldinga Bay; and Dry Creek Sands in
the Abattoirs Bore.
Age, Middle to Upper Eocene, Miocene, Pliocene,
win rm Examined, About 50 specimens, mainly from Peel's Bore (VL4,
Carcharias maslinensis sp, nov.
(Plate 2, Figs. 1-8)
Diagnosis. Teeth with very slender crown, circular cross-section al base.
Anterior teeth with very sinuous elongate crowns, twisted, Anterior cutting cdge
more prominent. Regular, deeply-incised,, longitudinal striatious. on imner face,
almost to apex. Pair of minute, conical lateral denticles, well separated from
crown, Root of anterior teeth with strong median boss. Lateral and distal
teeth straighter, erect, having roots with widely divergent Hattened Iwhes.
Description of Types
Holotype (F17260) (Pl. 2, Figs. 1, 2). A typical anterior tooth of Car
charias, but distinguished by extreme slenderness, prominent sinuosity and
axial twist. Jt is almost circular in section at the hase, where the cutting edees
are nonexistent, but becomes semicircular towards the apex, with the outer face
being almost flat. Anterior cutting edgé begins about two millimetres above
base and is quite sharp; posterior culting edve begins aboul 5 uum above hase
but is less prominent and rather blunt. The outer face is smooth except for a
small sub-median plica, the inner face is strongly convex and longitudinally
striated to within 3 mm of the apex. Striae are fine, regular, almost parallel,
bifureating towards the apex. A very small, curved-conical lateral cusp js
preserved on the anterior side of the crown, some distance beluw the base,
The root is strongly bitid with narrow lobes at about 40°, separated by a
prominent median boss with a deep nutritive pil at the apex.
Dimensions. Total height 20-8 mm; crown height (alony outer face) LAS
mm, inward displavement of apex ce. 10 mm; base width 4°35 nun; base thiek-
ness 4-0 mm,
Paralypes
(a) Anterior teeth (V35) (Pl. 2, fig.3). Similar to holotype, but most have
lost the lateral cusps.
(b) Lateral teeth (V1S) (PL 2, figs, 4a, 4b). A number of teeth found
in the same Naracoorte bore assemblage are deemed to represent the Iateral
and posterior teeth of C. muastinensis sp. nov. because they are similar ta the
anterior teeth in slenderness, stviation, and lateral cusps. They ditter in being
evect, with equal margins, a relatively short crown, and widely-bifurcating, Ilat-
lobed roots Two groups cau be separated; one, having relatively wide main
cusps, presumabh- represents teeth from the upper jaw, the other, lower jaw
teeth, This. conclusion is. based on observations on the variation of teeth in the
jaws of the living Carcharias arenarius Ogilby, which observations also explain
the differences in roal form and the shortness of the crown in the lateral teeth,
FOSSIL ELASMOBRANCIL TEETII OF S.A. 147
Judging by the gradation in size and form of both lateral and anterior tecth
and the preservation, it is considered that they might represent one individual,
Occurrence, E, & W.S. Bore No, 5, Naracoorte (426 f[t.).
Depositories of Types. Holotype: Dept. of Geology, University of Adelaide,
F17260. Paratypes; Geological Suryey of South Australia, V15, V35.
Observations. The teeth differ from Lamne attenuata Davis, which Chap-
man reported (1918) from the Lower Aldingan Beds, by possessing striations
on the inner face, and a twisted sigmoidal shape of the crown, Chapman and
Pritchard (1904) describe Odonlaspis dttenuata (Davis) as having a striated
inner face, but none of the material seen in the Victorian National Museum
agrees with the specimens of C. maslinensis. The lateral tecth of C. maslinensis
are similar to yery smal] specimens of C. macrotts.
TABLE 1.
DIMENSIONS OF TYPES
Anteriars Upper Laterals Lower Laterals
height | width | thickness height with, | thickness] hei hit width | thickness
is
holotype paratyped paratypes
16°8 4-5 4-0 $3 4e8 2-4 1-7 3°09 2:3
72 4+] 2-0 79 340 2+5
paralypes
16-1 4-9 4-1 6-1 3:3 2-0 7-0 2-4 Be,
12+1 Bb 2d 648 3-4 2-0 5-8 #0 1-7
12-1 h-6 2:9 7-0 3:7 23 13 2-8 2-L
iO a+4 2-5 6-5 2-8 2-1 5-8 24 1-7
9-9 he | 2-3 Ad) 27 1-8 T- a0 2-3
12-6 3-0 2-5 5-1 2-9 1:7 yao | 3:0 2-0
Red 2-8 2rd 4 33 1-5
fo 2:9 1:6
a-6 2-3 1:7
7+6 4-5 23
C. maslinensis is commonly found in the Eocene deposits of South Australia,
and appears to have undergone some evolutionary change, as specimens from
the Blanche Point Marl and Port Willunga Beds (lower part) are stouter than
those from the older Tortachilla Limestone and Knight Formation. It is a
common constituent of the assemblage of crowns in the basal grit member of the
Tortachilla Limestone, but most identified specimens are of anterior teeth, for
it is difficult to distinguish the lateral tecth on crowns alone, Three poorly pre-
served specimens from the Strathalbyn assemblage could page 28 be
reworked from underlying Eocene strata during the Miocene transgression.
Occurrence. Peel's Bore, 390 ft, Co. Rohe, Hd, Ross, Sec, 19; E. & WS.
Bore No. 5, Naracoorte, 426 ft: a farm bore near Lucindale, 200 ft; a farm bore
near Kingston, 715 ft; basal grit of Tortachilla Limestone at Maslin Bay, basal
part of Muloowurtie Formation, Yorke Peninsula, Blanche Point Marl; lower
part of Port Willunga Beds; and Strathalbyn (cemetery road cutting) Manoum
Formation equivalent,
Age. As recorded so far, C. maslinensis ranges from Middle to Upper
Eocene, and possibly to Lower Miocene, unless reworked.
Material Examined. About 50 specimens from south-eastern bores, includ-
ing the types F17260, V35, and V18. Another 50 crown enamels from the
Tortachilla Limestone, and several teeth from other levels.
148 N. 5, PLEDGE
Carcharias cf. cuspidatus (Agassiz)
(Plate 3, Figs. 5, 18, 13)
Lamna cuspidata Agassiz, 1843. p. 290, pl, 37a. figs, 43-30,
Odontaspis cuspidata Woodward, 1889, p. 125.
White, 1931, p. 53, figs. 19-44,
Diagnosis, Teeth very similar to C. macrotus oxcept for absence of striae
on inner face, Sometimes more robust than corresponding teeth of C. macrotus,
but smaller. One pair of small, pointed, lateral cusps. Nutritive foramen in
deep cleft.
Observations. A large number of teeth, many from Peel’s Bore, fit in this
diagnosis, but most are wanting roots and/or lateral cusps. Those which are
complete come within the range of variation for the species as illustrated in
White's figures, but altogether they make up a rather heterogeneous collection
which may represent several species. It has not heen possible to separate them
into more satisfactory groups.
Occurrence. Peels Bore, 390 ft. (Knight Formation); basal part of Tor-
tachilla Limestone, Blanche Point Marl, Port Willunga Beds in the Willunga
Basin; and Strathalbyn (Mannum Formation equivalent).
Age. Middle Kocene to Lower Miocene, in South Australia,
Material Examined. Almost 100 specimens, including about 50 from Peel's
Bore, and many crown enamels from the Tortachilla Limestone, and Strathalbyn,
Carcharias cf. rutoti (Winkler)
(Plate 3, Pig, 14)
Otodus futoti Winkler, 1876, p. 6. pl, 1. figs. 3, 4,
Odontaspis rutati Woodward, 1889, -:p. 361.
Chapman and Cudmore. 1934, p, 125, pl, 10, fiz, 97,
White, 1931, p. 49, fizs. 4-12.
_ Diagnosis, Teeth small; robust but not very high, with faces smooth, but
there may be vertical plications on outer face. At least two pairs of sharp lateral
cusps—outer ones insignificant. Root with prominent median boss. Outer
base-line of crown re-entrant.
Observations. Small specimens similar to C. rufoti have been recovered
from the Blanche Point Marl, where the appurently casily detached lateral cusps
are preserved. No specimens have been seen having three pairs of lateral cusps
as in Winkler’s description, but from White’s figures, such occurrences are un-
common—only one of his nine figures shows three pairs of cusps. One specimen
ascribable to the species was found in the Peel's Bore assemblage.
On the specimens available, the main cusp is more or less inclined, fairly
broad, and relatively thin. The denticles are conical, sometimes compressed, and
sometimes incurved. towards the main cusp.
Chapman and Pritchard (1904) recorded similar teeth from Victoria as
“Lamna bronni’, which is a Cretaceous form, and it has been suggested that
C. rutoti is the correct determination,
Occurrence, Blanche Pomt Marl, Blanche Point, Maslin Bay, Knight
Formation, Peel's Bore (390 ft.).
Age, Middle and Upper Eocene.
Material Examined. Two teeth from Blanche Point, one from Peel's Bore.
FOSSIL ELASMOBRANCH TEETH OF §&.A. 149
Carcharias dubius (Agassiz)
(Plate 3, Fig. 10)
Luning dubia Agassiz, 1843, p. 295. pl. 37a, figs. 24-26.
Odontaspiy dubia Clikman, 1964, pl. 25, figs. 12, 13. 16, 17, 19» pl 27, Ags, 18-23.
Diagnosis. Teeth very similar to C. contortidens, but lack striations on
inner face. Crown rounded, subeylindrical at base, not flattened towards, apex.
Single pair of lateral cusps: cylindrical, clongate, very acute. Root and lateral
cusps rarely preserved.
Observations. A number of teeth having similar characters to this form
were found in the Peel’s Bore Assemblage. The crowns are elongate and acu-
minate, with little or no. cutting edge on the lower part. Width is only slightly
greater than thickness. Rovt large, prominent median boss, lobes at about-90°.
The teeth show signs of being polished, but not of excessive wear, They are
similar to those figured by Glikman (1964) except that the root is not as broad.
Occurrence. Peel's Bore (390 ft.), County Robe, Hd. Ross, Sec. 19.
Age. Middle Eocene.
Material Examined. Five teetly from Peel's Bore.
Carcharias sp. indet.
Observations. Five entirely unworn tecth, having some resemblance to
C. dubius and C, cuspidatus, but differing in detail, were found in the Naracoorte
Bore Assemblage.
The teeth are small, having narrow erect crowns and a pair of large conical
lateral cusps. They differ from C. dubius in having sharp cutting edges, also
on the denticles, and widely divergent root lobes, The median boss is pro-
minent. One tooth is from an anterior central position, while another is
posterior and is developing a second pair of denticles,
Qceurrence. E. & W\S. Bore Na. 5, Naracoorte (426 ft), Knight Formation
equivalent.
Age. Middle Eocene.
Material Examined. Five teeth from the Naracoorte Bore.
Carcharias cf. ensiculatus (Davis)
(Plate 3, Fig. 15)
Lamna ensiculaia Davis, 1858, p, 18, pl. 3, figs. 6, 7.
Diagnosis. Teeth small, strong, erect, Crown enamel divides just above
hase, at point marked by constriction, and extends over upper part of root
lobes. Faint indication of lateral cusps.
Observations, This form is represented here by a single specimen which
well illustrates the peculiar flaring and bifurcation of the lower part of the
enamel. No lateral cusps can be seen, The root is strong and deeply bifurcated
at about 90°; the inner side is flattened and bears a prominent nutritive pit,
However, the root is not as large as in the figures of Davis. His material came
from the “Oamaru Formation” (Oligocene) of New Zealand, which is consider-
ably younger than this specimen,
Occurrence. E. & W.S. Bore No. 5, Naracoorte (426 ft.).
Age. Middle Eocene,
Material Examined: One specimen.
150 N. $. PLEDGE
Genus CancuAnroLamNa Hora, 1939
Diagnosis, Teeth having form of Lamna and bearing close resemblance to
Carcharaides, but being distinguished hy osteodont structure, less developed
lateral cusps, finely denticulated margin, and bhint apex.
Carchariolamna cf. heroni Hora
(Plate 3, Fig. 16)
Carchariolamna heront Wora. 1939, p, 203-203, pl. 13, figs. 1-4.
Diagnosis. Teeth similar to Carcharias or narrow specimens of Lamna sp.,
erect, broad base, apex blunt; margins finely denticulate, from apex almost to
base. Jateral denticles small, blunt, incipient. Root broad.
Observations. The specimen at hand consists only of the crown of a taoth,
It agrees with Hora’s description and figures, cxcept that the apex is more
acuminate, and no flaring is seen at the base. The margin is well preserved,
and differs from that of Carcharoides in the fineness of the dentes,
Occurrence. Marion No, 2 Bore, 225 ft., Sturt River Valley. Another tooth
of this form was found by Howchin in a quarry at Mt. Gambier.
Age. Lower to Middle Miocene (Batesfordian-Balcombian).
Material Examined. Two specimens.
Family ISURIDAE
Genus Lamma Cuvier, 1817
Diagnosis. Teeth as for Carcharias Rafinesque, but principal cusps broader,
and lateral cusps larger and stouter, Cutting edges do not extend to base of
crown,
Lamna obliqua (Agassiz)
(Plate 4, Fig. 1)
Otodus obliquus Agassiz, 1845, p. 267. pl. 31, 36, figs, 23-27
Lamna oblique. Woodward, 1889, p, 404,
White, 1931, p. 46, fig. 3.
Diagnosis. Teeth robust, large; crown moderately compressed, acuminate,
one pair of broad Jateral cusps, sometimes a second smaller pair in distal teeth,
Both faces smooth, Rarcly, cutting cdges faintly denticulated, Prominent
median boss, nutritive foramen not in groove.
Observations. This species is rare in Australian Terltiarics, and only two
specimens have been available. The larger specimen is a distal tooth having
a short crown and two pairs of stout lateral cusps. The root is stout and widely
bifurcated with Daintel: lobes. The other specimen, from Peel's Bore, is small,
more oblique, with one pair of small denticles.
Qccurrence. The larger specimen is part of an old collection and is labelled
“Miocene,? Deepwell, Murray Scrub”. However, the preservation is similar to
that of teeth from the Knight Formation of the Murray Basin, The smaller
specimen is from Peel’s Bore, near Robe,
Age, Middle or Upper Eocene.
Material Examined. Two specimens.
FOSSIL ELASMOBRANCH TEETH OF S.A, 131
Lamna cf. apiculata (Agassiz)
(Plate 4, Fig. 2)
Otedus apiculatus Agassiz, 1843, p. 275, pl. 37, figs. 32-35,
Lanma apiculate Chapman, 1918. p. 13, pl. 5, figs. 17-20. pl. 6, fig. 4,
Chapman and Cudimore, 1924, p, 126, pl, 10, figs, 28, 29.
Diagnosis. Moderate size, triangular, relatively thin, more or less oblique;
outer face with some small vertical plicae at base; pair of short, blunt, biconvex
luteral cusps. Root strong; widely divergent, pointed lobes. Detached crowns
very similar to Isurus hastalis, but have greater median thickness.
Observations. Only a few of the specimens at hand still retain the lateral
cusps; identification of others is uncertain. Many specimens are small, and may
represent a different species, as they occur in only one horizon—the basal part
of the Tortachilla Limestone. The form occurs. sporadically through the Tertiary.
Occurrence. Basal member of Tortachilla Limestone, Maslin Bay; Blanehe
Pojnt Marl at Aldinga Bay, Port Noarlunga and Moana; Strathalbyn; Morgan
Limestone Lype section (Cadell Marl Lens); Morgan township; base of T.oxton
Sands, Waiketie.
Age. Upper Eocene to Pliocene.
Material Examined. Fourteen specimens.
Lamna cf. erassidens Agassiz
(Plate 4, Fig. 4)
Lamnea. crassidens Agassiz, 1843, p. 292. pl. 33, figs, 8-21,
Odontaspis (?) crassidens Woodward, 1889, p. 373.
Lamna cressidens Chapman and Cudmore, 1924, p, 126,
Diagnosis. Teeth robust, large, rather spatulate outline; outer face gently
convex; inter face strongly convex, medially depressed. Root strong, long widely
divergent lobes. Crowns yery similar to Istwus desorii,
Observation. A single tooth fits this description. The crown is erect, and
spatulate, with the inner face strongly convex but medially depressed. It is
placed in Lamna because the cutting edges do not extend to the base, and it
is tuo robust to be put in Carcharias, There is no sign of lateral cusps, The root
has widely divergent lobes.
Occurrence. River Mnrray cliffs, probably near Morgan.
Ave, “Lower Murravian” ie, Lower Miocene.
Material Examined. One specimen.
Lamna vincenti (Winkler)
(Plate 4, Fiz, 3)
Lama compressa Agassiz (pars). Agassiz, 1843. p. 290, pl. 37a, figs. 41-42.
Lamnea vincenti (Winkler), Woodward, 1899. p. 10. pl. J, Ags, 21, 22.
Leriche, 1905, p. 125-127, pl 6, fus. 36-51.
Leriche. 1936. p. 390, pl, 2G. figs, 14, 15.
Diagnosis. Teeth strongly compressed, crown expanded at base, inner
face smooth: upper teeth oblique, lowers erect; one pair of Jateral cusps,
moderate size, well separated from crown, divergent; small outer pair of cusps
in more distal teeth.
Observations. Two undoubted specimens of this species were found in the
Blanche Point Marl by Mr, R. |. F. Jenkins, and several incomplete teeth may
also be referable to the species. Tt is distinguished from the fourm C, cf. ruloli,
whicli is also present, by the compressed crown and straight outer base-line.
Occurrence. Blanche Point Marl, Blanche Point
Age. Upper Eocene, Carter's Unit 2.
Material Examined. Two complete teeth and several crowns.
152 N. 8. PLEDGE
Genus [surus Rafinesque, 1810
Diagnosis. ‘Teeth generally large: crown compressed, triangwar, acute,
erect or slightly oblique, margins entire, extend right to base; no lateral cusps.
Root thick; short, rounded lobes.
Tsurus cf. hastalis (Agassiz)
(Plate. 4, Fig. 5)
Oxyrhina hastalis Agassiz, 1843, p, 227, pl. 34, figs, 3-13, 15-17.
Woodward. 1889, p, 385.
Istetus hastalis Ishiwara, 1921, p, 62, pl, 10, figs, 1-32.
Chapman and Cudmore, 1924, p, 129. pl. 10, fiz. 30.
Oxythina hustalis Leriche, 1957, p. 27, pl. 3, figs. 1-8.
Diagnosis, Teeth large, broad, compressed; outer face flat or concave,
sometimes with plicac; root short, almost straight, blunt-ended, Anterior teeth
very large, triangular, thin erect; upper laterial teeth inclined. Lower teeth
thicker, more erect.
Observations. This species has been the subject of much “s liting and
“lumping”. Agassiz’s species Oxyrhina hastalis, O. triganodon, and O. plicatilis
are now commonly included in the synonymy, and Ishiwara (1921), for instance,
has included a number of Jordan’s Californian species, As a result, Isurus
hastalis consists of a number of forms, and allocation to the species is sometimes
uncertain. Reference to the teeth of the living Isuropsis mako (Whitley)
(= Isurus glaucus (Miller and Henle) ) shows that such a wide range of forms
is to be expected,
Few undoubted specimens of J. hastalis arc al hand from South Australia,
although they are abundant in the Victorian Miocene. The teeth show a similar
range in form to those figured hy Ishiwara (1921), but they are often con-
siderably smaller. They also have a long time range, and may therefore represent
several species. Some specimens assigned here may be incomplete teeth of
Lamna apiculata,
Occurrence, Blanche Point Marl, and lower Port Willunga Beds in Aldinga
Bay (uncertain identification); Strathalbyn cemetery road cutting; Cadell Marl
Lens, Morgan type section; Morgan township; Mannum; Mt. Gambier,
Age. (?) Upper Eocene to Middle Mioccne.
Material Examined, Eight good specimens and numerous enamel fragments
from Strathalbyn.
Tsurus desorii (Agassiz)
(Plate 4, Fig. 7)
Oxyrhina desorii Agassiz, 1843, p. 202, pl. 37, figs, 8-13,
Woodward, 1889, p. 382.
Tsurus desorit Chapman and Cudmore, 1924, p. 132, pl. 10. fi, 32.
Oxyrhina desorit Leriche, 1957. p. 26, pl. 44. fixs. 18-23.
Diagnosis, Teeth with crowns narrower than I. hastalis, broader than T.
retroflexus, sigmoidal curvature in upper anterior teeth. Outer face nearly flat,
inner very convex, but medially depressed,
Observations. The few specimens available are generally in a poor state
of preservation, consisting of detached crowns only, There are few really
distinctive characters, but the teeth fit roughly between the limits set. However,
there 2 ap to be a tendency for the forms hastalis, desorii aud retriflexus to
interyrade, and these determinations must therefore he regarded cautiously.
FOSSIL ELASMOBRANCH TEETH! OF S.A, 153
Occurrence. The better preserved teeth are of uncertain origin, but appear
to have been collected from the Murray Cliffs—possibly from the Cadell Marl
Lens near Morgan. Others, consisting of enamiel only, were collected from the
road cutting near the Strathalbyn cemetery, ic. Mannum Formation equivalent.
A tooth ascribable to I, desorit was also found in the Peel’s Bore Assemblage.
Age. Middle Eocene (?), Lower Miocene,
Material Examined. Hight specimens.
Isurus retroflexus (Agassiz)
(Plate 4, Figs, 8, 9)
Onyrhina retroflexa Agassiz, 1843. p. 281, pl. 33, fig. 10.
Woodward, 1889, p, 389.
Isurus retroflecus Chapman and Cudmore, 1924, p, 130, pl. 10, fig. 31.
Oxyrhina retraflexa Leriche, 1957, p. 30, pl, 45, figs. 9-11.
Diagnosis. Isurus teeth, rather short, robust, narrower than J, desorii. An-
terior crowns strongly incurved. Inner face very convex, not depressed; outer
face slightly convex in lower teeth, flat in upper teeth. Lateral teeth curved
backwards to angle of jaws.
Observations. Teeth of this form are very similar to those of I, desori, but
are marked by greater incurvature, and by convex outer faces. One specimen
of an upper anterior tooth is almost complete, and shows a basal expansion of
the crown enamel onto the root.
Occurrence. One specimen, a lower anterior, was found in limestone at
Myponga in a posthole at the Myponga cheese factory. The others are from
less well defined localities: Aldinga Cliffs, Murray Cliffs, according to their
labels,
Ave. Upper Eocene (?)—Oligocene, Lower Miocene.
Material Examined. Seven specimens.
P Isurus sp.
(Plate 4, Fig. 10)
Description. A number of similar teeth, represented only by the enamel of
their crowns, have been found in two different formations,
The crowns are elongate, narrow, relatively thin, and slightly inclined. The
apex is blunt. The margins are entire, reaching right to the base, but are blunt;
although worn, they show little sign of having been sharp. The outer face is
slightly convex, medially depressed at the base, and extends below the normal
base-line in a wide “tongue”, The inner face is more convex, smooth,
The slenderness and the character of the outer face make its allocation to
Tsurus rather uncertain.
Occurrence, Basal grit member of the Tortachilla Limestone, Maslin Bay;
and Strathalbyn cemetery road eutting—Manmnum Formation equivalent.
Age. Upper Eocene, and Lower Miocene.
Material Examined. Fifteen specimens.
Genus GArncnarovon A, Smith (in Miller and Henle, 1838)
Diagnosis. Teeth large to very large, triangular, serrate or dentate margin;
outer face flat, inner face convex; sometimes with serrate lateral cusps.
fd N, 5, PLEDGE
Carcharodon megalodon (Charlesworth)
(Plate 4, Fig. 12)
Carcharias megalodon Charlesworth, 1837, p. 225, fig, 24.
Carcharodon megalodon Agassiz, 1843, p. 247, pl. 29,
McCoy, 1875. Dec, 2. pl, 11. fig. 4, p. 9
Woodward, 1889, p. 415,
Ishiwara, 1921, p. 65, pl, 10, fe. 33, pl. 11, figs. 1-6. pl. 12, figs. 1, 2.
Chapman and Cudmore, 19294, p. 133.
Lericha, 1957. p. 32, pl. 3, figs. J-1S.
Diagnosis. Very large, broad triangular, robust; outer face fat; apex slightly
everted; no distinct lateral cusps. Margin with rounded dentes.
Observations, This is one of the best known of fossil sharks’ teeth, mainly
because of its large size. The sharks growing these teeth have been estimated
to haye reached 30 metres in length, with a jaw gape of two metres. Although
found in large numbers in some parts of the world, only relatively few teeth
have been found in South Australia, An upper right lateral tooth, in the Depart-
ment of Geology collection, has a crown about 45 mm high, and shows marked
inclination towards the posterior, A fragment of enamel from the Strathalbyn
locality may also belong to C. megalodon. The teeth are marked by a spatulate
outline, the margins being convex towards the apex, and concave towards the
base.
Occurrence. The specimens at hand come from Barber's Quarry, Mount
Gambier, and also trom Strathalbyn. Others have heen found at Pt, MacDonnell,
Lake Bonney (S.E.). Morgan, and. Blanchetown, and elsewhere in the Murray
Basin,
Age. Lower to Middle Miocene,
Material Examined. Seven specimens, iichiding five in the South Australian
Museum,
Carcharodon auriculatus (Blainyille)
(Plate 4, Fig. 11)
Squalus anviculatis de Blainvile, 18L8. p, 384,
Carcharodon auriculatus Agassiz, 1843, p, 254. pl. 28. figs, 17-19.
C_ angustidens Agassiz, 1843, p, 255, pl. 28, figs. 20-25. pl. 30, fies. 2, 3,
McCoy. 1875, Dee. 2. pl LL, figs. 2, 3. p. 5.
GC. auriculatus Woodward, 1889. p. All,
Chapman and Cudmoere, 1924. p. 134.
C. angustidens Leriche. 1957, p. 32, pl. 3, fig. 14,
Diagnosis. Teeth robust, smaller and narrower than C. megalodon; single
pair of serrated lateral cusps, especially large in lateral teeth, which have very
narrow, rather oblique crowns.
Observations. The specimen at hand is almost complete, lacking onlv the
apex of the crown. The crown is crect, and narrow in its upper part, but flares
suddenly about 1 cm above the base. The inner face is convex but medially
depressed. he Jateral cusps are conrpound, ic, their outer edges lave two
or more major points, all of which are serrated. The serrac are quite pointed,
whereas the specimens of C, mevalodon at hand have rounded dentes. The root
is strong, with widely divergent, flattened lobes.
Occurrence, Port Willunga Beds, Aldinga Bay. Others haye been found
at Mount Gambier and Tailem Bend,
Age. Olivocene to Lower Miacene.
Material Examined. Seven specimens, including six in the South Aus-
tralian Museum.
FOSSIL, ELASMOBRANCH TEETH OF 5,A, 155
Carcharodon carcharias (Linnaeus)
(Plate 4, Fig, 13)
Squalus carcharias Lirmaens, 1758, p, 235.
Carcharodon rondeletii Miller and Henle, 1841, p. 70.
Woodward, 1889, p. 420,
Carcharodon carcharias Ishiwara, 1921. p. 68, pl. 17, fig, 3.
Chapman and Cudmure, 1924, p. 135.
Diagnosis, Carcharodon teeth, but relatiyely small, reaching 40 mm height;
broad triangular, thin, straight margins, no lateral cusps.
Observations. The specimen at hand consists of the main part of the crown.
The margins Hare only slightly at the base, and are irregularly denticulated with
well-separated rounded dentes. The outer face is slightly convex, but medially
depressed. This species is still found in South Australian waters, and has world-
wide distribution,
Occurrence. Dry Creek Sands, Abattoirs Bore, Hd. Yatala.
Age, Upper Miocene, Recent.
Material Examined. One specimen, plus jaw of living shark.
Carcharodon sp. indet.
(Plaie 4, Fig. 14)
Observations. A small tooth, obviously belonging to Carcharodon sp., has
been found in the Blanche Point Marl. The apex and much of the root are
missing, and the total height of the remainder is about 15 mm. The crown is
uite thick (6 mm), and almost complete, except for apex and extremities of
the base, and is inclined to the posterior. Only one of the cutting edges is
preserved intact, and shows moderate-sized round-ended dentes. The tooth
evidently comes from the posterior part of the jaw. Of the root only the central
portion remains, preserving a median boss with a shallow groove.
Occurrence. Blanche Point Marl, Blanche Point.
Age. Upper Eocene—Carter’s Unit 2.
Material Examined, One tooth. Jenkins’ collection,
STRATIGRAPHIC DISTRIBUTION
It is seen that, although sediments covering most of the Tertiary are present
in South Australia, the known distribution of fossil sharks” teeth within them is
discontinuous. This is mainly a collecting bias, due to favourable lithology for
preservation and subsequent discovery, although assemblages from bores come
from discrete levels.
A number of assemblages from units in which fossil sharks’ teeth are rela-
tively plentiful are listed below. They are treated in stratigraphic order.
a. Knight Formaiion (lower part): Pecl’s Bure, Co. Robe, Hd. Ross, Sec.
19, 890 ft., E. & W.S, Bore No. 5, Naracoorte, 426 ft.
Age. Middle Eocene,
Species. “Notidanus” serratissimus, Myliobatis spp., Galeecerdo sp. indct.,
Carchorias macrotus, C. contortidens, C, maslinensis sp. nov., C. cuspidalus, C.
rutoti, C. dubits, C. ensiculatus, Lamna obliqua, Isurus cf. desorii.
b. Tortachilla. Limestone (basal grit), Maslin Bay.
Age. Aldingan (Upper Eocene), Carter's Unit 1.
L663 N, & PLEDGE
Species. Carcharias macrotus, C, euspidatus, C. maslinensis sp. nov.
Lamna cf. apiculata, Isurus (?) hastilis, Isurus (2) sp.
These are all preserved as only the enamel shells of the crowns.
e. Blanche Point Marl. Blanche Point and other places.
Age. Aldingan, Carter's Unit 2.
Species. “Notidanus” serratissimus, Pristis cf. cudmorei, Myliobatis sp.,
Carcharias macrotus, C, contortidens, C. ct. cuspidatus, C. cf. rutoti, C. masli-
nensis, Lamne apiculata, L. vincenti, Isurus cf. hastalis, Carcharodon sp. indet.
d. Strathalbyn, cemetery road cutting (IId. Bremer, Sec. 2548).
Formation. Sublittoral equivalents of Mannum Formation.
Age. Lower Miocene.
Species. “Notidanus” sp. indet. (fragmental), Curcharoides ef. totuserratus,
Carcharias macrotus, C, ct, cuspidatus, C. (2) maslinensis, Lamna apiculata,
Isurus hastalis, 1. desorti, Isurus (?) sp. (same as in Tortachilla Limestone),
Carcharadon megalodon.
e. Marion No. 2 Bore, Sturt River Valley, Hd. Adelaide (depth 255 ft.),
Formation, In or near Munno Para Clay member. Port Willunga Beds.
Age. Batestordian-Baleombian (Lower Miocene), Carter’s Units 9-10,
Species. “Noatidanus” sp, indet. (fragment), Carcharhinus cf. collatus,
Carchariolamna cf. hereni, Carcharias contortidens, C_ cuspidatus.
_ £. Cadell Marl Lens, Morgan Limestone (type section, 4 miles downstream
from Morgan).
Age. Lower Middle Miocene, Carter's Unit 10.
Species. Carcharhinus aculeatus, Galeocerda aduncus, Hemipristis serra,
Carcharias macrotus, C. ef. cuspidatus, Lumna apiculata, L. crassidens, Isurus
hastalis, I. desrii, [. retroflexns, Cavcharodon megalodon.
g. Dry Greek Sands, as in Abattoirs Bore, Tennant’s Bore.
Age. Upper Pliocene (Yatalan).
Species. Myliobatis mourabbinensis,* Carcharhinus (Prionodon) aculeatus,*
Carcharias ct. macrotus, C, contortidens,? Lamna sp., Carcharodon carcharias.
As the accompanying Table 2 shows, some species are restricted to rela-
tively short-lime ranges. This is partly an artificial zonation, caused by differen-
tial preservation and paucity of specimens. Some species have short time ranges
on a world seale, and the specimens at hand fall into them; others have long
time ranges and may be represented by only a few specimens. Im several cases,.
teeth apparently fall outside the accepted time ranges for the species with which
they are compared.
The following species are apparently restricted to the Middle Eocene in
South Australia: Carcharias dubius, C. ensiculutus, Lamna ubliqua.
Apparently restricted to Upper Eocene: Pristis of. cudmorei, Lamina vincenti.
Found in both Middle and Upper Eocene: “Notidanus” serratissimus, Car-
charias maslinensis, C. cf. rutoti.
* These species were reported hy Créspin and Cotton (in Miles, 1952) from the Abattoirs
Bore, but the matcrial has not been seen by the author.
157
FOSSIL ELASMOBRANCH TEETH OF S.A.
Pieistocene dune limesands |/Blanchetown Clay [Hindmarsh Clay . _ fie & pases a F
af 5a Ps “ oe, ae $10
Py | Yatalan | Norwest Bend Fm flee SOry Ck 3 se ee Math we oe we BM Oe gus arte fe tte b
Wocene Katimoan [Toxton Sands | Sk Sk Jeter ge GP AR ob rb New aeerden et bal eat acted
4 - Boukpurnong Bed eft 6 ca me the ne hw Bg pe teed ry ee 4
+ pe pete ne Fe ewe Mut eae fl eet fe 4
U.Miocene Mitchellian ar a er ae] Pa ee i oe oe oe Pe ene ey
Rg ie ae ee ead ty ee pies gp Pte
Bairnsdalian Pata Lst. « ‘ . t+ * ‘ . i a ny * rene + “2 A te oe ee
M.Miocene a Gy WE Ww an e® “dateetlate 4p PR od ain Aether 4
Balcombion wt Os le Se eee ee ate 9 le CR) Fe nt ot
Morgan ist, p Pare] * x x ae
18-19 Na “- 4 og ae WS gi tcrg* «8 *eg wget ene +} 'e
™
ro. e S we » = - 4 wey . 2 a ee sew Mw he
* |
L Miocene & | wh Pretec fae gw arly Ste te Fi the ee et bah
3 Mannum Fm, Port at Fes Ee oe ee ns cat ge
e
5 Ettrick 7 3 ‘ es 98 @ sf «4 Cr ey . Dew % tre ta FH
U Oligocene 3 Witlunga Ae on GS a Ba a hk whee RP es cals be She be oe
§ Fm. wt gg! ete ge fe OIE ee ee, . oes
. ~ ' , 4 .
al-32 Janjukion an gk gt ee cmt ett dip diate te pupae Cartons
LiOligocene s Fa + wh bee ue EO ee ede te b> Wee Dee f *5
lh - ¢ = a
g Beds 8 os one = 8 b&b Bem ew ee ta idee ee ad Soe
ay-a6 Ranmork = sport pe lap AS Ae a ae ea ee eee nee eee EB BS
— 5 7 tg Woks Gg Bitte 2 hie Bana ete Bees
FS] Krisns Buccs et td db Bie gen gee tae BERS
U Eocene 2 Blanche Point SP te Pa ee 2 EE eB tees op pet ot SS
ra Beds Marl ar o- a3
-- - . oe . . . ee ste . . soe ome as oe , wr
shal 2 x i Be =
ee : TY] Sth Maslin Ss. EE at ete wat pres sues ZB Q%
Johonnian Formation 4: a Se ye ee Dele Fe te hee TP ERSB
M Eocene Pi EZ 3 8 Te SISESAI RL Be oy ee « Add
ws’? ----- 4 R a eR
yrs. et
ae Austration ||| GAMBIER MURRAY — |] St. VINCENT § eg £ 7 ¥ 3 g gz
Teazs Stages | ll] EMBAYMENT BASIN BASIN e *¥ = 38 38 € * 4 P 5
3 ~~ as uu >
a & Re § 2 & & iS 2 Eee e ge $$ oe See
a Suv © e s es ¢ * S&S
2 “Z| corretetion ofter Ludbrook(1967) Correlation % ea» z = 2 o£ = ef ges $ : $32 b 835 Bek
s = of the Tertiary Rocks of the Australasian Keyion”, 4 & ae & & 5 eb ae. & a8 fr “yy Sind oz 5 5
3 & in “Tertiary Correlations ond Climate Changes in BS % 3 & 3 = g $8 B35 2 S$ eust 28a 3 ry seo
- E = i. = a if & rm a 3 a3 ;
the Pucific, Symposim 25. Sendai, Jepan, 22 ¢ FS 8u & Bd & Sucduuu § Sana 8-2 Sus
158 N.S. PLEDGE
Found only in Gligncene; Carcharodon anrienulatus.
Apparently restricted to Lower aud Middle Miocene: Carcharhinus collatus,
Carcharoides totuserratus, Hemipristis serra, Galeocerdo aduncus, Carehario-
Jamu cf, heroni, Lanina ef. crassidens, Carcharodon megaladon.,
Apparently restricted to Pliocene (and later); Carcharodon carcharias.
Miocene to Pliocene: Carcharhinus aculeatus.
The other species oceur during both Eocene and Miocene, and some range
into the Pliocene, They raise the presently insoluble problem of whether such
forms indeed represent single species.
In comparison with the list of species given by Chapman and Cudmore
(1924), some notable absentees are seen for South Australia. Heterodontus,
represented in Victoria hy four species, has not been recorded, and there are
fewer myliobatids. There are also fewer Carcharhinid sharks represented, and
such species as Galeocerdo latidens and Sphyrna prisca have not been revo.
nized. These omissions are apparently the result of unfavourable sedimentary
environments combined with madcquate collecting in the requisite stratigraphic
evels,
The time is not yet ripe to establish vones based on sharks’ teeth asser-
blages as Glikman has done, although a large collection from any one locality
would indicate the appropriate Cainozoic epoch. Although many sharks are
pelagic, it is doubtful whether their teeth could be accurately used for wider
than regional correlation.
ACKNOWLEDGMENTS
Grateful thanks are given to Dr, N. H, Tadbrook, of the Palaeontology
Section, Geological Survey of South Australia, who kindly allowed the author
to stndy the Survey's extensive collection of teeth, Various other people made
collections ayailable for study or helped in other ways; Dr, D. W. P. Corbett,
Mr. C. J. Glover and Mr, H, Mincham of the South Australian Museum of
Natural History, Mr. T. Darragh of The National Museum of Victoria, Mr.
J, M, Lindsay of the Geological Survey of South Australia, Miss S. Summer,
Messrs, R, J. F, Jenkins, W. J. Stuart, J. Brooke, M, R. Walter and R, Wright.
Thanks are also given to Prof. M. F. Glaessner and Dr. M. Wade, who
kindly read and criticized the manuscript.
REFERENCES
Acasstz, L. J. R., 1843, Récherches sir les Poissons Fosyiles, Vol. WI. Neuchatel,
Amecuino, £., 1906. Les Formations Sedimentaires du Crétacé Supéricur et du Tertiare de
Putegonie, An. Mits, nae, Buenos Airey. ser. 3, vol. 8.
BratwyauLe, H. D. ve, 1818. Poissons Fossiles, Nouv, Diet. W'Hist. Nat. 27,
Cuavean, F.. 1913. Note onthe Oecurrence of the Cainozaic Shark, Careharvitles, in Vietoria-
Viet. Naturalist, 30, pp, 142-143.
CitAuman, F., 1917. Some 'fYertiury Fish Teeth. Proc, Koy, Soc. Vict. 29 (ms.), pp. 134-141.
Cuararan, F., 1918. Cretaceous and Tertiary Fish Remains frm New Zealand. NZ. Geol.
Surv., Pal. Bull, 7.
Carman. F.. and Cunmonr, F. A. 1924, Sone Cainozoic Fish Remains, with a Revision
of the Growp, Proc, Roy. Soc. Vict.. 36 (1.5.), pp, 104-163,
Cuarman, F,, and Prircranp, G. B.. 1904, Fossil Fish Remains from the Tertiaries af Aus-
tralia, Part I, Proc, Roy. Soc. Vict., 17 (1s8.), pp. 267-297.
Crarceswonrn, E., 1837. Notice of the ‘Teeth of Carcharias megalodon Ovcurring in the
Kied Crag of Suttolk. Mag. Nat, Hist. (ns), 1, pp. 225-228. ;
Tavis, J. W., 1888, On Fossil Fish Remains frow the Tertiary Formations of New Zealand.
Sci. Trans, Roy, Dublin Sow... ser, 2, 4, pp, 1-62..
FOSSIL. FLASMOBRANCH TEETH OF S.A. 159
Eastman, C. RK. 1901, Systematic Paleontology, Pisces. Maryland Geol. Surv, Ment.
Tiocene, pp. 98-110.
Eastman, ©, BR. 1904. Systeriativ Paleontolagy of Minvene Deposits of Muryland, Pisces.
Maryland Geol. Surv. Mem., pp. 71-93.
Crimsrax, L. S., 1964. Akily Paleogena i ikh strativraficheskoe wunchenie, Akad. Navk
SSSH,
Hooyun, D. A, 1954. Pleistocene Vertebrates from Celebes. IX Elasmobranchii. K. Ned.
Akad. Wetens. Prow. Ser. B, 57, pp. 4735-485,
Horna, S. L.., 1939. On Two Small Collections of Fossil Fish Remains from Balasore, Orissa.
Rec. Geol. Sury. India. 74, pp. 199-215.
Isurwana, ¥., 1921, Fossil Shark Teeth from the Neogene of Japan, Sci. Rep, Tohoku Inip,
Univ. Ser, 2 (Geol,), 5, pp, 61-74.
Jorpan, D. S., and Buar, GC, W., 1918. Supplementary Notes on Fossil Sharks. Univ, Calif,
Publ, Bull. Dept. Geol., 7, pp. 243-256.
aaa > M... 1902. Les poissons paléocénes de Ja Belgique. Mém. Mus. roy. Hist, ‘nat.
Be Be, .
Lenicne. M., 1905, Les. poissons éocénes de Ja Belgique. Thid,. 3.
Lenwenge, M., 1910. Les poissons aligocénes de Ja Belgiqne. ITbid,. 5,
Lenicns, M,,. 1926. Les poissons neogenes de la Belgique. Ibid. ser, 1. 32.
Lericue, M., 1936. Les Poissons du Crétacé et du Nummolitiqae de Ande. Bull. See.
Géol, France, ser. 5, 6 pp. 375-402.
Lewicne, M,, 1957. Tes Poissons néosénes de Ia Bretagne de l’Anjou ot de la 'Touraine.
Mém. Sou. Ceol. France, ser. 5. 81.
Lericur, M., and Casirn, K., 1954, Les Fausies ichthyologiqie marine du Néogéene dos
Indes orientales. Schweiz, paldont, Abh.. 70.
Linnsay, J, M., and Snerreny, R. CG. 1966, Muuno Para Clay Member. Geol. Surv, & Aust,
Qoart. Geol, Notes, 19, p. 7.
TLinwanis, C., 1758. Systema Naturae. ed, LO. p, 235,
McCoy, F,, 1875, Prodromus of the Palaeontology of Victoria, Dec, 2: 8-10. Geol. Surv. Viel.
Mrs, K.. 1952. Geology and Underground Water Resources of the Adelaide Plans Are.
Geol, Surv, &. Aust. Bull. 27, p. 234.
Miitun, J.. and Henue, F, G, J., 1841. Systematische Beschreibung Plagiostemen, Berlin,
Noernixe, T.. 1901. Vhe Fauna of the Miocene Bods of Burma. Geol. Surv, India, Mem, 1,
pp, 372-378.
Scere, T. D,. 1968, The Marine and Freshwater Fishes of South Austraha. Handhook of
flora und Fauna of South Australia, Govb. Printing Office, Adelaide,
Winrr, EJ. 1926. Eouene Fishes trom Nigeria. Geol. Sury. Nigeria, Bull, 10.
Wie, E, L, 1930. The Vertebrate Faunas of the English Eocene. Vol Lo Brit, Mos, (Nat,
Thist.),
Woonwann, A. S.. 1886, On the Palaeontology of the Selachian Genns Notidanny Cuvier.
Geol. Maz,, Dee. 3, 3. pp. 205-217,
Woonwann, A. 5. 1889. Catalogue of Fossil Fishes in the British Musewn (Nat. Hist.), Pt, 0,
Wouvwanp, A. 5. 1899. Tueth of Sharks and Skates fran English Eocene J’ornations:
Proc, Geol, Assoc., 16, pp. 1-14.
Zain, Ke von, 192% ‘Texthook of Paleontology, vol. IL revised by A. Sinith Woodward
(1932), pp. 50-08.
EXPLANATION OF PILATES
(All figures of inner fuer except where stated }
Puave |
Tutra Glass Orthocdonta (all 2 x natural size).
Fig, 1. “Notidenus’ serratissinius Ag. Blanche Point. Macl ( F17262),
Fig, 2, “N2 ef. serratissimus Ag., Nurecoorte No. 3 Bore, 426 ft. (VG).
big. 3. “Notidanuy”? serratissimus Ag, Blanche Point Marl (P17284 and Jenkins collestion).
Pic, 4. Myliohatis spp., toothplites, articulating surfaces, Naracoorte No. 3 Bore: (V41).
Fig, 5. Myliobatis sp. caudal spinc. Blanche Pot Marl (VAG).
Fig, 6, Pristiy c& cudmorei Chap., rostral tecth, Blanche Point Marl (F172835. FITSLS).
Fie, 7, Carcharhinus cf, collatus (Eastman), Marion No, 2 Bore, Sturt River Valley (17279,
¥17312-P17314). ,
Fig, 8. C, aeulwatus (Davis), River Morray Clits, probably Morgan (PT7270)..
Fig. O. Hemipristiy serra Ag. Cadell Marl Liews, 4 tiles 8. of Morgan (ELT288 }.
Fig, 10. a. Calvoeerdo adunens Ag., Morgim (E17275). hb. Guleocerdo sp., locality mnknown,
possibly near Morgan (FI727L),
Fiz. 11. Carcharoides of. tutuserrales Ameghing, Strathbyn (117287).
160
Fig,
Tig.
Fig,
Fig.
Fig,
Fig,
Fig,
Fig,
Fig,
Fig.
Vig.
fig. ]
ig.
Fiz.
N. 8. PLEDGE
Puare 2
Carcharias maslinensis sp, noy. (all 2 x natural size)
1-4, E. & W.S. bore No. 5, Naracoorte (426 ft.), Knight formation.
I.
2.
tw
,
4,
5
6,
8,
as
Holotype, immer face (17260).
Nolutype, posterior profile.
Paratypes--anteriors (V35).
Paratypes (V1S): a. upper laterals: b, Jower Laterals.
. Maslin Bay, basal. Tortachilla Liniestone—crown enamels only: 4, upper laterals
(F17295-F 17300); b. lower laterals (F17301-F 17307); c. anteriors (F17289-F 17294).
7. Anterior tecth, Blanche Point Mar] (Carter's Unit 2), Maslin Bay (Brooke and
Jenkins collections).
Anterior tooth, lower Port Wilhmga Beds (Carter's Unit 3), Aldinga Bay (£17267).
Puatr 3
(Natural size except where stated )
. 2, 3. Careharias macrotys (Ag,), large specimens, upper and lower anteriors. Blanche
Point Marl, Maslin Bay (F17308-P17311, and Jenkins collection),
* 6. a pyran (Ax.), Peel's Bore (390 ft.) near Robe; Knight Formation
VIG, 4
. C. cl. macrotus (Ag.), Naracoorte Bore No, 5 (426 ft.) (V49).
. C. cf, macrotus (Ag.}, Peel's Bore (390 ft.) (V53),
. Caroharias sp, indet.. Naracoorte Bore No, 5 (V32).
. CG, dubius (Ag.), Peel's Bore, near Robe (V27),
. C, cantortidens (Ag.), Peel's Bore (V14).
2, C. cf. euspidatus (Ag,). (?) Blanche Point Marl (£17264).
. GC. cf. cuspidutus (Ag.), Blanche Puint Marl, Maslin Bay (Jenkins collection).
. C. cf. rutoti. (Winkler), Blanche Point Marl. Maslin Bay (F17263 and F17265).
C_ensiculutus (Dayis). Naracoorte Bore No_ 5, x 2 (V36): a. inner face; b. outer face.
. Carchariolamna cf. heroni Hora, Marion No, 2 Bore. Sturt River Valley. x 2
(F17280).
PuatTe 4
Family Isuridae (all natural size).
. Lamna abliqua (Ag.), “Deep yell, Murray Scrub”, probably from Eocene Knight
Formation. equivalents (£17269).
. L. apiculata (Ag.), Blanche Point Marl, Maslin Bay and Witton Bluff, Pt. Noarlunga
F17261. F17266, and Jenkins collection),
. L, tineenti (Winkler), Blanche Point Marl, Maslin Bay (F1728G6 aud Jenkins col-
lection ).
. L. ef. erassidens Ag., Murray Cliffs, probably near Morgan (P172725,
. Tsures hastalis (Ag.), Murray Cliffs, probably Cadell Marl Lens near Morgan
(F17273),
. 1. ef, Aastalis (Ag.), basal Port Willunga Beds. Aldings Bay (F17268),
. 1. desorii (Ag.). Strathalbyn, crown enamels only (1° 17282, F17315).
IT, retroflexus (Ag.), upper right lateral tooth, Port Willunga Beds, Reddin’s Bore,
Gawler River (270 ft.). (Photo by courlesy of J. M, Reddin,)
. 1, retroflesus (Ag), anterior tecth, Murray Clills, near Morgan (F17274): a. inner
face; b. profile.
. Isurus (?) sp., basal Tortachilla Limestone, Maslin Bay (1°17283. 17316, F'17317).
. Carcharodim auriculatuy Ag... Port Willunga Beds, Aldinga Buy (117276}.
. G. megalodlen Charlesworth, Barbers Quarry, Mt, Gambier (F17277).
. €. carcharias (Linn,), Dry Creek Sands, Abattoirs Bore, Pooraka (F17278).
. Carcharodon sp. indel,, outer face, Blanche Point Marl, Witton Bluff, Port Noarlunga
(Jenkins collection).
PLATE |
PLEDGE
S.
N,
9
N, S. PLEDGE PLATE
So
N. S. PLepce PLATE 4
STRATIGRAPHY OF LATE CAINOZOIC DEPOSITS IN
SOUTH AUSTRALIA!
BY J. B. FIRMAN”
Summary
The stratigraphy of late Cainozoic deposits in southern South Australia is set out for sedimentary
basins and adjoining uplands in terms of environment and time.
Middle Tertiary tectonic movements initiated late Cainozoic sedimentation. Tectonic movements at
the end of the Pliocene produced a pattern of lineaments, which set limits to the inland penetration
of rising seas, and controlled trends of stream courses and lake and continental margins.
The Pliocene-Pleistocene boundary is well defined locally by faunal evidence, and regionally by an
erosional break, which separates strongly ferruginized estuarine and fluvio-lacustrine sands from
fluvio-lacustrine clays.
The sequence of Pleistocene shallow marine and littoral deposits on the continental margin is
subdivided into lower, middle and upper beds. Correlation with inland continental deposits is
facilitated by through going soil stratigraphic units containing silcrete, ferricrete and calcrete.
The shift from a cooler, wetter climate of the Pleistocene to a warmer and drier climate in the
Recent is recorded inland by extensive dune sheets.
STRATIGRAPHY OF LATE CAINOZOIC DEPOSITS IN
SOUTH AUSTRALIA‘
by J. B. Firman?
[Read 10 August 1967]
SUMMARY
The stratigraphy of late Cainuzoic deposits in_ southern South Australia
is eet out tor sedimentary basins and adjoining uplands in terms of environment
and time.
Middle Tertiary tectonic movements initiated Jate Cainozoic sedimentation.
Tectonic movements at the end vf the Pliovene produced a pattern of lineaments
which set limits to the inland penetration of rising seas, and controlled trends
of stréam courses and Jake and contmental margins.
The Pliocene-Pleistocene boundary is well-defined locally by faunal evi-
dence, and regionally by an erosional break which separatcs strongly ferru-
ginized estuarine and fluvio-lacustrine sands from: fluyio-lacustriné clays,
The sequence of Pleistocene shallow marine and littoral deposits on the
continental margin is subdivided into lower, middle and upper beds. Correla-
tion with inland continental deposits is facilitated by throughgoing soil strati-
graphic units containing. silerctc, ferrierete and calercte.
The shift from a cooler, wetter climate of the Pleistocene to a warmer aml
drier climate in the Recent is recorded inland by extensive dune sheets.
INTRODUCTION
This. paper sets out the stratigraphy of Jate Cainozoic deposits in the
southern part of South Australia, The study includes the Murray, St. Vincent
and Spencer Gulf, West Coast and Fucla Basins and the adjoining uplands,
Wark has been concentrated on the southern margin of the continent where
marine, transitional and continental deposits and related land surfaces oceur
together, The paper is essentially a study of physical sequences, and is. a
necessary preliminary to systematic radiometric dating and the study of changes
in climate, flora and. fauna during the late Cainozoic.
On the stratigraphic table, rock units are organised according to environ-
ment and timc. The reader secking detailed information oun the identification
and description of stratigraphic units and their relationships, is referred to the
writers’ papers quoted herein. Tabulations in these papers suinmarize much
of the evidence used as a basis for correlation in this paper. Environments
shown on the table depend upon different models; geomorphic, sedimentary,
geological and palaeontological concepts have been employed at various places.
A uniform treatment of environments must await a unified system of classifica-
tion. Those deposits which show the influence of climatic zonality are empha-
sized on the table and in the text.
1 Published hy permission of the Director of Mines, South Australia.
2 Geological Survey of South Australia,
Trans. Roy. Soo, §. Aust, (1967), Vol. 91,
166 J. B. FIRMAN
LOCALITY MAP— MINOR LOCALITIES
Place. names referred to in text and shown on Locality Map by numbers.
1, Avondale Homestead 20. Lake Torrens Craben 39. Molineyirx, Hundred of
2, Barossa Valley 22. Loxton 40. Point Labatt
3. Blanche Point 23. Lipson Reach 41. Port Augusta
4. Blanchetown 24, Lyndhurst 43. Port Wakefield
5. Bookpurmong 25, Maree 44, Renniark
6, Boston Bay 26, Marmon Jabuk 45. Ripon, Hundred af
7. Bungunnia Iontestead 27, Millewa 4G, Sir Joseph Banks Group
8. Chowilla 28. Parilla 47, Spencer Gulf Graben
10, Coomandook 29, Monoman Creek 45, Swan Reach
11, Coorong Lagoon 30, Moorlands 49. Tartanga Island
12. Fulham 31, Naracoorte 50. Telford Railway Station
13. Etadunna 32, Nildottic Sl, ¥Yallunda
14. Dry Creek 33. Nilpena 52. Callana
15, Hall Bay 34, Maslin Bay 53, Coffin Bay
16, Hallett Cove 35, Noarlunga-Willonga Basin 54. Lockleys
17. Hindmarsh 36, Padthaway 55. Marina
18. Karoonila 37. Pinnarso 56, Smart Bluff
19. Kimba 38. Peehinga 57,, Coomonga
The study is based on cxamination of rock sequences revealed by drilling,
regional stratigraphy and terrain analysis, and by investigations in support of
mineral exploration, hydrology and soft-ground engineering, Although the
paper has been prepared with the views of other workers in adjoining areas
in mind, no attempt has been made to review their work in detail.
STRATIGRAPHY AND GEOLOGICAL EVENTS
TERITARY
Tectonics and Sedimentation
The nature and extent of Jate Cainozoic scdiments in South Australia
reHects earlier tectonic movements which caused the retreat of the Miocene
seas and initiated dominantly: clastic deposition throughout the remainder of the
Cainozoic. For. asummary of early Tertiary tectonic events the reader is referred
to Webb (1958).
Sedimentary basins in Sonth Australia contain about 1,000 feet of Tertiary
sediments, overlying Permian and Cretaceous rocks resting on a Precambrian
basement. Tertiary biostratigrapby bas been descrihed for the basins generally
by Ludbrook (1958, 1959, 1961 and 1963). The basins, as they occur now,
were shaped during the Caimozoic. Within each basin, a very strong trend trom
Miocene marine through transitional to continental sediments is apparent.
Quaternary stratigraphic units are remarkably extensive, and the most important
occur in hasins on the seaward margin of the State where transitional sequences
link the stratigraphic record of the ocean basins and the continents.
Upland Ferricrete and Sedimentary Equivalents
Although this paper deals mainly with late Cainozoic stratigraphy, the
processes responsible for some of the silcrete and ferricrete so prominently
displayed in the late Cainiozoic landscape were in operation much earlier. One
of the more important events during the Lower Tertiary was the formation of
1 Massive vesicular. cellular o¢ concreti¢mary ironstone overlying mottled and pallid zanes
is termed “laterite”, Detailed stratigraphic stndies reveal that this classic profile contains
layers that have been formed in dillerent ways at diferent times, the profile being as oli] as
the first weathering of the parent rock, ‘hese considerations Joad to the use of ferricrete
as a non-genetic term for the ironstone in this and other profiles.
STRATIGRAPHY OF LATE CAINOZOIC DEPOSITS 167
NORTHERN
ss
ten,
QUEENSLAND
WESTERN AUSTRALIA
oO
uy
a
=
3
a
=
wy
2
VICTORIA
Miles ¢ 300 Miles
; + oe:
Kilometres O 400 Kilometres
£ - = |
67-387 J.B. Firman S.A. Department of Mines
165 ]. B. FIRMAN
ironstone in “laterite” profiles on old land surfaces in the npland areas moarginal
to the basins. Lower Tertiary ferricrete is recorded by Harris and Oliver (1965)
above and below Lower Tertiary sediments in the Barossa Valley, Ferricretes
associated with the remnants of a high-level “peneplain” surface in the Mt,
Lofty area have been described by Rix and Hutton (1953), Thomson anc
Horwitz (1961), and by others quoted in Webb (loc, cit.) and Wells (1966)
The Yallunda Ferricrete of the Lincoln Uplands (Johns, 1961; Firman, 1967)
occurs in a similar geomorphic situation to the “peneplain” ferricate of the Mt,
Lofty-Olary avd Flinders Ranges,
The sedimentary sticcession in the Murray Basin has been examined for
equivalents of the ferrierete in upland areas: oolitie siderite and “laterite” have
been recorded in the Lower Pliocene Bookpurnong Beds; ferruginous beds aril
cappings are found in the Upper Pliocene Loxton Sands; “ironstone” is recorded
within the Upper Pliocene Parilla Sand and ortstein has been mapped at its
surface; upper beds of Parilla Sand in the South Australia-Victoria border region
are ferruginous and contrast with the non-ferruginous lower beds cropping out
in River Ruiray cliffs. Ferruginisation in Lower Pliocene basin sediments ma
correlate with the massive ironstone described by Gill (1958) in the Black Rock
Member of the Lower Pliocene Sandringham Sands in Victoria. | Ferricrete
(including ortstein) in Upper Pliocene basin sediments is correlated with
ortstein on the eastern slopes of the Mt, Lofty Ranges, Geomorphic evidence
shows that these deposits rest upon slopes incised through the “peneplain” ferri-
cretes, and are therefore younger, and sedimentary evidence—notably similar
lithology and close proximity to the Parilla Sand of the basin margin—suggests a
correlation between ortstein-hearing beds on the eastern slopes of the ranges
and the Parilla Sand of the type area in the Murray Basin.
Silerete has been described mainly from inland areas of South Australia
by Wopfner (1960, 1964), Wopfner and Twidale (1967), Stephens (1964),
Stewart (1958), and others, but it bas also been recorded on Yorke Peninsula
NOTES ACCOMPANYING TLE STRATICRAPHIC TABLE
Sedimentary Basing
A, Murray Basin, B, Mt. Lofty-Olary und Flinders Ranges. C. St, Vineent and Spencer
Basins. D. West Coast Basins, E, Eucla Basin,
Notes
1. For Pleistocene-Recent deposits, “Neritie’ is applied to shallow-water marine enviren-
ments identified from sedimentary and veomorphic evidence, und ranviny from high-
energy nearbeach situations fronting: the open ocean to low-energy near-heach situa-
tions within the Gulfs. For Plincene deposits, “Neritie’” includes epinuritic shallow
water Dry Creck Sands (Glaessner, M. E. and Wade, Mary. 1958) and marine shallow
water Bookpuroong Beds (Undbrook, N. IL, 1958 and 1961),
8, Soils are superimposed on the units with which they are associated stratigraphically,
Symbols in vertical bars show the time ranye, horizontal burs show the unit relationship.
3. Coorong Jayoon area,
4, Cottin Bay urea.
5. Deposits in the River Murray.
Port Wakufield, ;
7. Upper member contains several layers of moderately hard caleretes
4%. Sediments of the St. Vineent Graben,
9 Limestone at the top of Hallett Cove Sandstone at Marino, Hillett Gove, Blanche Toint,
10. Sand below limestone (0) at Hallett Cove und Muslin Bay.
1], Sedimentary equivalents of the upland ferricvetes on basin margios are shown Lelow
this line.
12, Deposits in the Barossa Vidley (Exainple from Rowlands Flat jn Tarris, Wook, andl
Olliver, J, G,, 1965}. ;
3, Callana und Smart Blull examples in Morbes, B,C, (1966),
1. Lincoln Uplands.
STRATIGRAPHY OF LATE CAINOZOIC DEPOSITS 169
LATE CAINOZOIC DEPOSITS IN SOUTH AUSTRALIA —-— STRATIGRAPHIC TABLE
ENV | RONMENT
#1 | LITTORAL, LAGOONAL, COASTAL LACUSTRINE, a
NERITIC ESTUARINE AEOLIAN PALUDAL FLUVIAL - COLLUVIAL INLAND AEOLIAN SOILS
7 = 1 EM Leachee candy
i ’ c, e zens
Shelly, Felsarvcite Carbonate sediments SEMAPHORE SAND Fea B50 Recent | ceca Regent & horitgns
tits Shell) sand D4 Salt crusts alluyium inal yands
—_—_|—
MOLINEAUX
SAND *
Soft ropy and
~ FULHAM SAND® columnar umisatet
BUNYIP. SAND * oP pyle
RECENT 4 , Voleante ash
at Mount Gambier Gays sod
alles in
initermontane
basins
Talus and slope
Geposits on
surtaces pest
Loveday. Soil
ST. KILDA FORMATION °°
LIPSON FORMATION
YAMBA FORMATION *
GOONAMBIDBAL FM." -
YAMBA FORMATION *°
o=6-0-6-0-0-0 4 ~c—o—a—o-o—o-| ff LOVEDAY SOIL*
Sheets of POORAKA CLAY < WOORINEN FORMATION’ B Horizons of coh
aealisn shell sand . OS™ nodular and platy
ae TELFORD GRAVEL x th Pe
Gypsiferous Soil "
4 - ‘ TERRA-KOSSA AND
. RENDZINA
Sand and MONOMAN Red-beown sand sheet
sandy clay:
AD LE
In-solution pipes” FORMATION: over calerete AP BLACK EARTHS:
RED. BROWN EARTHS
| 1 Calerece in Py
wy BAKARA SOIL
(os = = =
bs i ON” ;
i me ED aaa BRIDGEWATER TELFURD GRAVEL"
| Galereted shell sand Upper Member Lower" Member”
RIPON GALGRETE.
EISTOCENE =
Terrestyial
MIDDLE > | BUNGUNNIA.L3,* ats fp] Mancaniferous. seaming
: FORMATION *> fa N ard )
Lower Mumiber y i
Gypsum and Aw)
COOMUNGA FM. IMM gypaerovy aly
Caquina and calearenite ar base of
Bridgewaser Fornarien?
ZBLANCHETOWN CL
®
A |/_——___|,,, Soil horizons of
IF) naduiar carbonare
6, accumulation &
ea oLAY
Bodonone Soop soe
xe
COOMANDOOK FORMATION”
Sande at Lachieys © CHOWILLA SAND”
Limestone? HALLETT
“sand atte eine ESAS *) Talus and slope deposirs ‘
flanking ranges as ae ficet®
NORWEST BEND FM, * PARILLA SAND” |g aaa eeaaeacaa
Limestone at Fehery Bay?
ORY CREEK SANUS
and bedrock highs eee) Ferncrete
: : i: (oreste
isi
LOXTON SANDS
(Upper bed) *
LIOCENE | ; wa tt al
LOXTON SANDS
(ower bed) “
- ? ?
LOWER PLIOCENE-MIOCENE
ry Fider silere!
LIMESTONE OF VARIOUS ENVIRONMENTS: Hyrine GAMBIER LIMESTONE: SSS SRS
PATA spd MORGAN-MANNUM \imescone’? (imesvene ar Myponga, and MELTOW
LIMESTONE!” PORT WILLUNEA REDS,* and WULLARAON LIMESTONE. ©
TERTIARY 7 pmrote
:° oe) Older ferricreres
2 (YALLUNDA.
le! FERRICRETE
Shale with leaf of Lenco Uplate)
HFFERENTIATED
impresnons. in Silty and.
MURNPEOWIE fancy ays
Formation ®?
Ce
ewes 2 wy
170 |, B. PIRMAN
(Crawford, 1965) and near Kapunda (Dickinson and Coules, 1957) and Ade-
laide (Stewart, loc. eit.). Recent investigations on Islands of the Sir Joseph
Banks Group by the Geological Survey of South Australia and on Eyre Penin
sula from Kimba to Boston Bay (Firman, loc. eit.) have demonstrated its Oecur-
ened over a wide area in the southern part of (he State. Fluvial processes have
heen more active ou the southern margin of the continent, aud this may account
for the erosion of all but a few remnants of silerete in upland areas and foe
burial of silerete-bearing sediments on the basin margins. The occurrence of
silerete south of the arid zone demonstrates that silerete lormation is not re-
stricted to that zone. Other considerations, notably geologic age, the oced for
a high water table favouring silica accumulation, and the presence of extensive
ferruginous mottling in associated beds, favour a wetter chmate than the present.
The approximate stratigraphic position of a 2Lower Tertiary silerete has
heen shown at the base of the stratigraphic table following Forbes (1966), The
stratigraphic position of the Boston Bay Silerete {s uncertain, bul the unit ds
placed in the late Tertiary because of its position in the landseape and its rela-
tlonship to younger deposits (Firman, loc, cit.).
The silicified cap on the eroded surface of Parilla Sand in the Marray Basin
is placed in the Pliocene on the table, but it could equally well be a Pleistocene
feature, The land surface at the time of silicification is termed the Karoonda
Surface (Firman, 1966a).
In South Australia, clastic continental equivalents of late Tertiary marine
sediments have a distinctive lithology and configuration. ‘Their most charac-
teristic features are ferrugirfisation and the presence of extensive developments
of ferricrete, These features are not found in younger deposits of known
Quaternary age,
QUATERNARY
Late Pliocene-Pleistocene Tectonics
Faulting ocemred throughout the Tertiary and, by_ the lose of the late
Pliocene, a well-defined pattern of lineaments, including faults and major joints,
had heen developed, Some lineaments parallel older faults and have throws up
ta 200 fect, others are probably major joints. On photo-mozaics of the basin
areas the fractures usually occur as lineaments mendiseg roughly northwest and
northeast. The fractures occur in several sets and their intersection forms
shomboid blocks, At this time, the inland side of the basins was upwarped and
the seaward margin downwarped; the Mt. Lofty, Olary and Flinders Ranges
were further aplifted and the extent of the sedimentary basins was reduced;
limits were set to the inland penetration of rising, seas and the trend of river
courses and of lake and continental margins was established. The pattern thus
controls the tectonic and geomorphic framework of Quaternary sedimentation,
Pleistocene"
PLioceNE-PLEISTOCENE BOUNDARY
A long period of erosion and sub-aerial weathering at the end of the Ter-
Hary and the beginning of the Quaternary intervenes between a time of extensive
quartz sand deposition in the Pliocene and a time of extensive clay deposition
1 The South Australian seqnence has been subdivided so that the Middle Pleistocene
containy the Bridvewater Formution and associated ealeretes, Sedimentary evidence suggests
a short time-span for the Upper Pleistocene, and a long time-span for the Lower Pleistucene
when compared to the Middle Pleistocene.
STRATIGRAPHY OF LATE CAINOZOIG DEPOSITS I7L
in the Pleistocene. The period was interrupted locally by tectonic movements
(sec Twidale et al, 1967).
The sands at Lockleys in the St. Vineents Basin that underlie the Hindmarsh
Clay are placed in the Calabrian Stage at the base of the Pleistocene by Lid-
brook (1963), The Plioeene-Pleistocene boundary has therefore been placed
between the sands at Lockleys and the underlying Pliocene Dry Creek Sands.
This same break in the sequence has been found in the Hallett Cove Sandstone,
south of Adelaide, where Pleistucene fossiliferous limestone Gyerlies a lower
bed uf sand which, according to Ludbrook (pers. comm.), contains a fauna
equivalent to the Pliocene Yatalan fauna in the type section (see Twidale,
Daily and Firman, 1967). In other sedimentary basins the Pliocene-Pleistocenc
boundary has been supposed to lie directly below the Pleistocene mottled clay
sequence (Ilindmarsh Clay and equivalents), but the evidence from Leckley's
in St, Vincents Basin suggests that the boundary may lie deeper in the sequence
in other basins also (Firman, 19652).
On the south side of the Murray Basin on the Padthaway Archipelago, the
Coomandook Formation overlies the Parilla Sand whieh is equivalent to the Dry
Creek Sands, and is in turn overlain by the wedge of aeolian Bridgewater
Formation, The seas in whieh this unit was deposited, penetrated inland as
far as the Marmon-Jabuk scarp and the extension of a southeast trend to
Naracoorte, No sedimentary evidence exists for greater inland penetration of
any later Pleistocene high sea,
Althongh Tate (1877) refers to debris at Third Creek near Adelaide
... attributed to the action of glaciers”, South Australia appears to lie outside
the area of Pleistocene glaciation, Periglacial conditions may be indicated by
late Pleistocene Gilgai soils, which resemble patterned ground and have shrink-
and-swell structures that appear to be fossil, and by other structures in gravels
near Peebinga and in cemented loess near Moorlands that may be due to
trost-hieave.
oo
ConTINENTAL AQUEOUS SEDIMENTATION
Fluvial and lacustrine deposition now occurred over a wide area in the
southern Australian lowlands, In tectonic depressions flanking the Mt. Lofty-
Olary and Flinders Ranges, such as the St. Vincents Graben, Spencers Gulf and
Lake Torrens Graben, sequences up to 400 feet thick of irregularly bedded
sandy clay with abundant sand and gravel lenses were laid down, The Hind-
marsh Clay in the St, Vincents Graben is typical of the thick sequences and
iy comparable to the Shepparton Formation described by Lawrence (1966) in
the Riverine Plains of Victoria, In shallow basins, sequences about 50 feet
thick of regularly bedded sandy clay with a few thin beds of sand were de-
posited, The Blanchetown Clay in the Murray Basin, the Avondale Clay in
hasins adjoining the northern Flinders Ranges and the Ochre Cove Beds in
the Noarlunga-Wilhinga Basin (Ward, 1965) are zepresentative of the thin
sequences, Diprotodon (Howchin, 1918) and Afaeropus have been recorded
from these deposits.
‘Lhe widespread occurrence of the units suggests the transportation of large
amounts of fine clastics during a pluvial climate, Formation of gypsiferous
evapnrites and termination of clistic deposition marks a drier climate phase at
the end of this time.
Thin dolomitic micrites (Bungunnia Limestone of the Murray Basin, Nil-
pena Limestone cast vf the Torrens Graben and un the west flank of the
172 J. B. FIRMAN
Flinders Ranges) were Jaid down. The Bungtnnia Limestone was mentioned
in Tate, Prof, Ralph (1855), who described “Travertine cover of thin-hedded
sandy limestone (over) red and blue clay” (Blanchetown Clay) as long ago as
1885, A “Cypridiferous limestone” was collected from the Victorian Mallee im
1912 and matched with other limestones, notably a Diprotodan-hearing lime-
stone from near Geelong, by Chapman (Chapman, Frederick, 1936). In the
Murray Basin, the extent of the Bungunnia Limestone marker defines the lake
system, called Lake Bungunnia in Firman (1965b), which contains the Blanche-
town Clay. The position of the limestone high in the Murray River cliffs 50
to 100 feet above a river graded ty a modern higher sea-level, suggests a terrain
with less local relief and a lower seaward gradient than at present,
The position of the Bungunnia Limestone in the rock stratigraphic sequence
outlined on the table is reliahly established. Other similar limestones have not
vet been placed in sequence, Reconnaissance traverses suggest that a sequential
arrangement of Pleistocene freshwater limestones exists; this would begin inland
with the Bungunnia Limestone and extend south through younger Teshwater
limestones of the south-east (Blackburn, Bond, and Clarke, 1967) to modern
carbonate sediments described by Mawson (1929) and by Alderman (1964)
in the Coorong lagoon adjoining the Southern Ocean. The Bimgunnia Lime-
stone-Blanchetown Clay sequence is correlated with a limestone®-clay sequence
(Forbes, loc. eit.) in the Maree-Lake Callabonna area which includes the
Avoridale Clay of Firman (1967). The similarity of deposits suggests that the
climate during deposition of Bungunnia Limestone hundreds of miles inland
of the modern coast may haye been similar, in some respects, to that prevailing
today in the lower south-cast adjoining the Southern Ocean-
Aronian Drrosivion mv amr Coastan Zonr
After the withdrawal of the sea in which the Coomandook Formation was
laid down, the lower member of the Bridgewater Formation was deposited along
the southern coastal margin, Bridgewater Formation was defined mm Victona
and contains “Calcareous duncs and dune limestones” ({ Boutakoff, cigr On
the sonthern edge of the Eucla Basin the lower aeolian member abuts directly
against a fossil chff cut in Nullabor Limestone; on the west coast the lower
member lies on a steeply rismg shoreline; in the south-east, the few known
occurrences of the lower member are scattered across the Padthaway <Archi-
pelago; in the St. Vincent and Spencer Basins the formation lies across the
entrance to Spencer Gulf and Gulf St. Vincent, Within the Gulfs continental
aqueous sedimentation appears to dominate througliout the Pleistocene: ‘Tindale
(1461) refers to“, . Late Pleistocene time, when St. Vincent Gulf was a great
alluvial plain, extending down towards Kanyiwou Island”, A similar situation
throughout the Pleistocene implies a delicate balance between tectonics and
sedimentation and sets a low limit to Pleistocene high sea-levels,
PLEIstoceENeE. GRAVELS
Within the sedimentary basins a period of crosion is inferred from calcreted
deposits on fault-line scarps and erosion surfaces, In the Murray Basin, the
most prominent markers are pre-calerete stream putterns in the Pinnarew-
SNot to be confused with Jimestene af the Ohyocene Etadunna Formation (Stirton,
R. A., Tedford, RB. H., und Miller, A. H.. 1961).
€ Tindale, N, RB. (1961): Advent of Mau in Australia. Syinposluai on Ceoclrouvlogy
and Jand Surfaces in relation to Soils in Australia. Organised by the Australian Acaderoy
af Science,
STRATIGRAPHY OF LATE GAINOZOLC DEPOSITS 173
Karoonda area (Firman, 1966b), and calcreted granule conglomerate derived
from Bungunnia Limestone; in the St. Vincent-Spencer Gulfs area deep incision
is indicated by pre-calcrete erosion surfaces cut into Pleistocene mottled clays
( Firman, 1965a ).
Extensive deposits of gravel ocenr in ontwash fans flanking the Mt. Lofty-
Olary and Flinders Ranges, The main unit within the deposits was named
‘elford Gravel in Firman (1967), The unit appears to form a significant part
of the debris mantle described by Twidale (1967). Deposition of the gravel
began prior to formation of calercte. The unit overlies the Nilpena Limestone,
which is probably the Bungunnia Limestone equivalent in the Beltana area
Leeson, 1966)7. The gravel is better preserved and better developed inland on
the flanks of the Northern Flinders Ranges than it is on the Hanks of the Mt.
Lofty-Olary Ranges to the south. The increased thickness and extent may he
explained by increased run-off due to greater Lectonic uplift in the Northern
Flinders Ranges in a wet phase of the climatic regime prevailing at the time.
The coarse grain of the clastics and their spatial relations suggest a change
in base level as a cause of increased erosion: a major withdrawal of the Pleistocene
sea is therefore postulated, Confirmatory evidence is found in younger deposits
described later.
Riron CALcRETE aNnp Time Lipon Surrace
The Ripon Calerete is an unusual deposit which is very well developed near
Hall Bay on the West Coast. Its formation requires the following events; Move-
ment by wind of calcareous silt released from weathering profiles, drying lakes
and the exposed continental shelf to form a thin but extensive blanket of louss
on the landscape; development of soil carbonate horizons followed by ernsion,
breceiation of the carbonate horizons aud recementation; repitition of the process
and formation of nodular carbonate accumulations interbedded with cemented
clastic material. This mixed deposit of thoroughly cemented soil and sedimentary
material has heen wamed the Ripon Calerete. It is up to thirty fect thick in places,
and forms an extensive but thinner cuirass inland and on the southern continental
mnargin, The surface below which carhonate accumulation occurred prior to
renewal of aeolian sedimentation is termed the Ripon Surface.
Barwecrwater Formation — Upren MEMBER
A return of the sea led to renewal of aelian sedimentation in the zone where
the liver member of the Bridgewater Formation had previously been deposited.
As a consequence, the Ripon Calcrete separates the wpper and lower members of
the Bridgewater Formation and has some of the characteristics of an intraforma-
tional breccia,
The upper member contains horizons of moderately hard valerete separated
by lenses of weakly cemented aelion calcarenite or non-cemented aeolian shell
sand. The random arrangement of the carbonate layers suggests Lhat conditions
favourable for the formation of the Jayers prevailed throughout the time of
formation of the upper member in the Bridgewater Formation, and that the
process was interrupted near the coast by irregular aeolian sedimentation. Dune
shapes in the upper member are well preserved.
T Leeson, B. (1966). Explanatory Notes: The Geology of the Beltana 1-mile Militaty
Sheet. Geol. Suryey of 8.A. Rent. Book.
Iv4 J.B. TIAMAN
THe BAxAna Som
Snland, beyond the limits of marine ingressions, the Bridgewater Formation
sediments ure absent and the calcrete layers coalesce to form a vertically con-
tinuos zone of soil carbonate accumulation, in many places with Ripon Calcrete
at the base. Soil profiles that include this calcrete zone are called the Bakara Soil
(Firman, 1963a and 1964). The surface below which carbonate accumulation
occurred in the Murray Basin is called the Nildottie Surface. This surface is
re-named the Bakara Surface herein to cover both inland and coustal situations
in southem Australia,
The original A horizons of the Bakara Soil were later stripped and the
exposed calcrete was strongly indurated. Solution channels were then developed
and these were infilled with sands and sandy clays, This sequence of events
suggests that the sands and sandy clays in solution channels was formed much
Jater than the calerete. In some places a red-brown sand is found above the
calerete and in solution channels. This forms the upper part of a soil profile
described as “terra rossa” in Stephens, et al. (1941) and is comparable with
“fossil ‘soils, mostly of the terra rossa typo” in Fairbridge R. W-. and Tcichert,
Carl, (1952), The red-brown sands are comparable to reddened fossil soils
within ibe Bridgewater Formation. This. and the proximity of the sand to the
upper calcrete in Pleistocene Bakara Soil, suggests that the Pleistocene-Recent
houndary could be placed above the sand. There are good reasons, howver, for
placing the houndary even higher in the sequence.
GLANVILLE ForMaATION
A marine ingression during the last interglacial inundated the coastal zone
Firman, 1963b and 1966c). Marls with a fauna including Anadara trapexia
Suture 1954) were deposited within the gulfs and in low areas hetween dunes
of the Bridgewater Formation®. The sea penetrated as far up Spencer Gulf as Port
Augusta—the first marine ingression recorded in the Tertiary-Quaternary sequence
in that area (Firman, 1965a). Within Gulf St. Vincent, the high sea eroded the
Ripon Calcrele near Port Wakefield to form 4 beach eravel that lies about 20 feet
ahove modern sea-level,
A lime-cemented crust was formed on the Glanville Formation (Howchin,
1888). A similar lime-cemented crust occurs on the floor of Gulf St, Vincent,
which suggests a major regression of the sea in which Glanyille Formatian was
deposited, The lime-cemented crust js correlated with calcrete in Bakara Soil
(Firman, 1963b and 19652),
Lovepay Sar
The low sea at the end of Bakara Soil time led to accelerated erosion: Newr
the modern coast, aeolianite was re-worked, Inland, Bakara Soil profiles were
eroded, Carbonate silt released from the locss was incorporated in dune shects
near the coast, in quarly sand of the Woorinen Formation inland and in colluvial
* By courtesy of G. van Andel of Scripps Institution of Oceanography, shell from the
Glanville Formation at Port Adelaide has been C-14 dated al yreater than 45.000 years,
The absolute age is said to be within ten of thousands of years of the age given (Heath,
G. R,, pers. comm),
* Woorinen Formation way defined in Victoria by Lawrence, C, R, (1966). Only the
lower three of the five units recognised by Lawrence are mopped as Woorinen Formation in
South Australia,
STHATIGRAPHY OF LATE CAINOZOIC DEPOSITS WS
and alluvial formations such as the Pooraka Clay, The soil developed hy accumn-
Jation of platy and nodular carbonate accretions in these deposits is termed
Loveday Soil (Tirman, 19662), Reconnaissance traverses suggest that the Wid-
gellic Pama of the Hiverine Plains (Butler, 1956) may correlate with Loveday
Soil, This accession of carbonate silt is the last in the record and is comparahle
to loess in earlier Pleistacene deposits. The extensive sheet of shell sand mixed
with this carbonate silt on the West Coast most closcly resembles earlier
Pleistocene aeolian deposits. For these reasons the deposits containing Loveday
Soil are placed in the late Pleistocene,
Recent
Tne FLaAnprian TRANSGRESSION
The post-glacial Flandrian transgression is recorded in deposits below modern
sea-level, such as the Lipson and St. Kilda formations (Firman, 1966c), in marine
cliffs and beach depusits now stranded (Firman and Chugg, 1963), and in
drowned topographic features marginal to the stable shield in the West Coast
area,
Beach ridges vf course shelly sand form the youngest member of the St.
Kilda Formation”. These deposits are now stranded inland up to about ten feet
above modern sea-level. Together with stranded marine cliffs, the position of the
deposits marks a regression of the sea. The formation of deep off-shore channels
marks # low stand of the sca, perhaps slightly below modem sea-level, These
features are well developed at various places along the South Australian coast,
weat Lake Macdonnell for example, where they connect an older and higher
littoral environment with the modern coast.
Dux Formation
Aeolian deposition began in the Pleistocene with the Woorinen Formation,
and continued into the Recent when the Fulham Molineaux and Recent forma-
tions were deposited.
Each stage of dune formation has a characteristic colour; Woorinen Forma-
tion is pale red-brown, Bunyip Sand is red-brown, Molineaux Sand is yellow and
Recent sand is pale grey, Except for Woorinen Formation, in which the puler
colour reflects the admixture of carbonate silt with quartz sand, the shift in colour
is duc to successive removal of iron-oxide coatings on the quartz sand. This is
paralleled by a decrease in the amount of carbonate in alluvial horizons within
the dunes.
Although dune building was initiated at four separate times, minor re-working
of older deposits is apparent; Two phascs of dceyclopment occur within the
Molineaux Sand, and all the deposits are heing actively re-worked at the present
time in some places, Despite this minor re-working, the dune sands retain their
colour. This leads to the conclusion that the initiation of each major stage of dune
formation reflects an important change in environmental factors. The widespread
distribution of each formation suggests that change in climate itself is involved,
10 Shell from the base of the beach ridges in the Port Wakefield area has heen C-l4 dated
ut 3,300 to 4,200 years B.P. hy Scripps Oceanogruphic Institnte (Heath, G. R., pers. com.)
lif J. B. FIRMAN
Fuvertne Derosrrs!’ anp omnen Recess Sepiments
Recent sediments in the Murray River tract near Chowilla include deposits
of an older meander belt, a younger meander belt and bed deposits of present
river channels, which are now about 50 feet abnve modern sea-level. These te-
gether form a younger valley fill overlying the Monoman Formation, The Tar-
tangan Beds of Hale and Tindale (1930) near Swan Reach are tentatively
correlated with sediments of the older meander belt. The “Upper Beds” of Hale
and Tindale (loc. cit.) are tentatively correlated with sediments of the younger
meander belt in the Chowilla area.
During the time of dune building marked by Woorinen Formation, tributary
streams were incised through thin surficial deposits into the gypsiferous beds at
the top of the Blanchetown Clay. When the tributary streams dried, gypsum
precipitated on the floors of valley lakes was blown by the wind to form lunettes
and dine sands that interfinger with Woorinen Formation. Gypsiferous sediments
were also deposited at the top of the upper valley fill.
Modem deposits are shelly calcareous silts of the neritic zone, carbonate
sediments in the Coorong lagoon, quartz and shell sand of the coastal aeolian
tract, peat of the swamps, saline crusts of the ephemeral lakes, sands and gravels
of the present stream channels and thin light grey sand sheets on hill slopes and
veneering inland dunes.
ACKNOWLEDGMENTS
The author is indebted to Dr. Helmut Wopfiner, Mr. B. P. Thomson, Dr,
B, G. Forbes and other officers of the Geological Survey for critical reading of the
text. Messrs. C. Lawrence and P. Macumber of the Geological Survey of Victoria,
and Student Geologists N, S. Pledge, N, Duncan, A, Andrejewskis, A. Williams
and L.. Barnes of the University of Adelaide gave valuable assistance to the writer
during field work in the Murray Basin. Unpublished Departmental reports by
N, H. Ludbrook: D. H.. Stapledon and J. P. Trudinger, W. Johnson, M. N. Wiern
and KR, D. Steel, G. Roberts and others were consulted during preparation of the
text,
REFERENCES
Acvemuan, A, RB. 1964. Dolomitic Sediments and their Environment in the South-east of
South Australia, Geochimica ut Cosmachimica Acts,, 29, pp. 13555-1365.
BiAcksunn, G,. Bonn, R. D., and CrArxs, A. BR. P., 1967. Soil Development Assouiated with
Strsuded Reach Ridges in Swuth-east South Australia. C,8.LK.0, Aust. Div, Soils,
Soil Pub. 22.
Boutaxorr, N., 1963. ‘The Geology and Geomorphology of the: Portland Arca. Geol. Surv.
Vict, Mem, 22.
Buruer, B, E., 1956. Parna—an Aeolian Clay. Aust. Journ. Sei. Vol. 18 (5),
Charman, Freperice, 1936, Cypzidiferons Limestone tram the Mallee, Geol, Sarvs Viel.
Rec. V (2), pp, 296-298,
QCrayrorp, A. R., 1965, The Geology of Yorke Peninsula. Geol. Surv, S. Aust. Bull, 39.
Digxrxson, S. B.. and Coates, R. P., 1957. Geological Atlas of South Australia. 1-Mile
Series, Kapunda 1 inch to 1 mile (1:63,360).
Fausumoce, Avwenors W., and Teicuent, Cunt, 1952. Soil Horizons and Marine Bands in
the Coastal T.imestones af Western Australia. Jour, and Proc, Roy. Soc. N.S.W.,
TXXKVI (3), pp. 68-86.
11 Sub-fossi] wood frum the base of the younger valley fill at Chowilla Dam has been
C14 lated at 4080 + 100 years hy Professor Kigoshi at Gakushuin University, Tokyo, Shell
from the Tartangan Beds is dated at 6020 + 150 B.P. (Tindale, Norman B., 1957),
Mononiin Formation is tentatively correlated with the geomorphic unit “Coonainbideal I
sedanents” of Pels, Simon (1966).
SURATIGRAPILY OF LATE GATNOZOIC DEPOSITS \77
Finaran, J. B., 1963a, Quaternary Geological Events near Swan Keavh in the Murray Basin,
Seuth Australia. Quart. Geol. Notes 5, grol. Surv. §. Aust
Firman, J. B., 1963b. Quaternary Geclogical Evonts near Port Adelaide. Quart (Ceol.
Notes 7. geol. Surv. S, Aust.
Frraaran, J. B., 1964. The Bakara Soil and Other Stratigraphic Units of Late Cainozoic Age
in the Murray Basin, South Australia, Quart. Geol. Notes 10, ygeol. Surv, '$, Aust:
Firman, J. B., 1965a, Late Cainozoic Sedimentation in Northern Spencer Gulf, Sunth
Australia. ‘Trans. Roy. Soc, S. Aust, 89, pp. 125-131,
Fomran, J. B. 1965b,.. Late Cainozoie Lacustrine Deposits im the Murniy Basin, South
Austrilia. Quart. Geol. Notes 16, geol. Surv. S. Aust.
Finman, J. Bo 1965¢e, Geological Atlas of South Anstulia. Special Series: Sifiee Map
Pinnaroo-Karoonda 1 inch to 2 miles (1;126,720),
Freman, J, B., 19662. Stratigraphy of the Chowilla Area in the Murray Basin. Quart.
Geol, Notes 20. geol, Surv. S. Aust,
Kraaan, J. B., 1966b. Geological Aas uf South Australiu. Special Series, Subsnrface Maps
Vinnaroo-Kardonda, 1 inch to 4 miles (1:253,440),
Foca, J, B., 1966c, Stratigraphic Units of Late Cainozoic Ave in the Adelaide Plains
Basin, South Australia. Quart. Geol. Notes 17. geol, Surv, S, Aust.
Fiumtan, J. B. 1967, Late Camozoic Units in Sonth Australia, Quart. Geol. Notes 23.
weal. Sury, S. Anst.
Frist, J. B., and Cuuce, 1. 1963. Marine Erosion and Stranded Beach Deposits near
Port Wakefield, Quart, Ceol, Notes 8 geol. Surv. S. Aust,
Pounes, B.G., 1966. The Geology of the Maree 1:250,000 Map Area, Ceol, Surv. S. Aush
Rept, Invest, 28,
Gua, BP. DB. 1958. Dating of Caivovoie Nonanurine Rovks im Aastralia. ANZ, AS,
Adelaide Congress, 1058, Section C,
Hato, H, M., aud Trypare, \, B., 1980. Netes on some Hinnan Remains in the Towr
Murray Valley, South Australia. Ree. '§. Aust. “ius. Vol. 4 (2). pp. 145-218,
[iansis, W. K,, incl Onurver, J. G., 1965, The Age of the ‘lertiary Sands at Rowland Plat
Barossa Valley. Quart, Geol, Notes 3, weol. Surv. 3. Aust,
Howaus, W.. (558. Reniarks on 4 Geologival Seetion ut the New Craving Dock. Glanville
with Special Reference to a supposed Old Land Siuface now below Sea Level. Trars.
Rny, Sac, 8. Aut, 10,
Jiowesus, W.. 19t8. “The Geology of South Anstralia.” (Govt, Printer: Adelaide. }
Jornvs, RK, 196). Gealogy umd Mineral Reseurees of Southern Eyre Peninsula. Ceol, Surv,
S. Aust. Bull, 37.
hawnesck, ©, PP 1966, Cainoveice Stratigraphy und Structure of the Mallee Regie, Vietuiia
‘Trans. Roy. Soe, Viet, 79. pp, 517-533.
Luounoon, N. A, 1958, Stratigraphic Sequence in the Wester Portion of the Buclr Basin
Journ, Roy. Suc. West. Anst.. 41 (4), pp. 108-114,
Lupunoox, N, H,, 1959. A Widespread Pliovene Molluscun Farina with Anodootia in South
Australia. “Lrans. Roy. Soc. §. Aust. 82, pp. 219-253, pls. |-3.
}uimmaok, N. A, 1961, Stratigraphy of the Muray Basin in South Australia, Geol, Surv.
S, Aust. Bull, 36,
fhuentoox, N. IL. 1965. Correlation of the Tertiary Rocks of South Austrilia. Trans Ray
Soe. & Aust... 87, pp. 5-15.
Mawson, D., 1929. South Australian Algal Limestones in Process ol Formation. Opn,
Soc, London Quart, Jour, 85 (14), p. 613.
Pets, Saron, 1966. Tate Quaternary Chronology of the Riverine Plain of Southeststern
Australia. Jour. Geol. Soc. Aust, 13 (1), pp. 27-40.
Hrs, GC E.. and Hurton, J, F.. 1953, A Soil Survey of the Mnndred of Kuitpo in the Mlowit
Lolty Ranges of South Australia. S$, Aust. Land Tax Dept. Bull, 1,
Sree, R. C.. 1954. Geology. Ch. 4. pp. 19.28. in The Soils and Geoloyy of Adelaitle and
Bepurie (Attehison, G; D,, Sprigg. KR. C., and Cochrane, G. W.), Geol, Sup, 3.
ust. .
STsORERS, C. ¢., 1964, ‘Sileretes of Central Australia, Nature, Vol. 203, Nu. 4952, p, 1407
4inly,
dternens, C, G., Cnocxen, R. L,. Bureun, B. and Sxwrn, BR, 1941. A Soil and Land tee
Sorvey of the Hundreds nf Riddoch, Hindmarsh, Grey, Young avd Nangwarry, Caunty
Urey, Sonth Australia. Coun. Sci. Indnstr. Res, Avist. Koll, 142:
Stewart, G. A, 1955, Hardened Siliveous Layers in Deeply Weathered Materials.
A,N.Z.AA.S., Adelaide Congress, 1958. Section C..
Tate, Raven, 1877, The Ancient Physical Geography and Geology of South Australia.
sonth Aust. Lost. Lectures in $, Aust, Public Library Press Records.
178 J. B. FLIRMAN
Tate, Prov. Rare, 1885. Notes on the Physical and Geological Features of the Basin of the
Lower Murray River. Trans, Roy. Soc. §. Aust.. 7
Tuomson, B. P., and Morwrrz, K. C., 1961. Geological Atlas of South Australia. 4-mile
Series. Barker 1 inch tu 4 miles (1:253-440).
TixpaLE, Noxman B., 1957. Culture Suecession iv South Eastern Australia from Late
Pleistocune to the Present. §. Aust. Mus. Records, Vol, 13 (1). pp. 1-49
Twmare, C. RR. Darmy, B., and Fmotan, J. B.. 1967, Discussion: Enstatic and Climatic
History of the Adclaide Area, South Australia, Jour. Geol, (in press).
Twiware, C. R., 1967. Hillslopes and Pediments in the Flinders Ranges, South Australia,
in “Landform Studies from Australia and New Guinea” (Eds, J. N. Jennings and J, As
Mabbutt). A.N.U, Press.
Wann, W. T. 1965. Eustatic and Climatie History of the Adelaide Region, South Australia.
Jour, Geol.. 73, pp. 592-602.
Wess, B. P., 1958. Summary of Tectonies and Sedimentation. Ch. XIL pp. 136-143, én
Geology of South Australia. (Edited M. F. Glaessner and L. W. Parkin,) Adelaide.
163 pp.
We tts, C. B., 1966, A Composite Mip of the Soils of Metropolitan Adelaide. C.ST.R.O,
Aust. Soils and Land Use Series 49.
Worrner, H.. 1960, On some Structural Developments in the Central Part of the Grest
Artesian Basin, Trans, Roy, Soc, S, Aust. 83, pp. 179-193.
Woernen, O., 1964, Tertiary Duricrust Profile on Upper Proterozoic Sediments, Granite
Downs Area. Quart. Geol. Notes 12. geol. Surv. S. Aust.
Worrner, H., and Twipace, C. BR. 1967. Geomorphological Tlistury of the Lake Eyre
Basin, in “Landform Studies from Australia and New Guinea” (Eds. J. N. Jennings amd
} A) Mabbutt), A.N.U. Press,
EXPLANATION OF PLATE
PLate }
Mig. 1. Murray Basin. Boundary Point near Millewa: (1) Loveday Soil, (2) Bimgunnia
Limestone, (3) Blanchelown Clay, upper and lower members. (4) Silivified furru-
zinous sandstone at top of Parilla Sand. (5) Talus. (6) Parilla Sand.
re
Pig. St, Vincent Basin. Blanche Point in the Willunga-Noarlunga sub-basin area: (1)
Ochre Cove Beds equivalent to the Blanchetown Clay. (2) Hallett Cave Sandstone,
upper bed of PPleistocene liniestone overlying a lower bed of Pliocene sand. (3)
Blanche Point Marls.
Fig. 3. West Coast Basins Arca: (1) Ripon Calerete, (2) Bridgewater Formation, lower
member, (3) Reddened soil horizons. (4) ‘Talus.
Fig. 4. Murray Basin, Renmark: (1) Recent soil. (2) Ball and sheet calerete, (3) Bun-
minnia Limestone, Himmer marks top.
J. B. Firman PLATE
J. B. Firman PuatEe 1 (continued)
THE INFLUENCE OF ENVIRONMENT ON TWO SPECIES OF
LAND-SNAILS IN SOUTH AUSTRALIA
BY D. E. POMEROY*
Summary
Helicella virgata and H. neglecta are the most widespread of a number of species of exotic land-
snails in South Australia. An analysis of their distribution and abundance by multiple linear
regressions showed that the presence of organic matter in the soil was most important for H. virgata
(it could not be tested for H. neglecta), and that there was a strong correlation between the
availability of calcium and the numbers of both species. The availability of moisture was significant
too, but the number of hot days in summer was markedly not so. The effects of land use, proximity
to man. and type of vegetation were of relatively minor importance. The method gave satisfactory
results, and might well be applied to other studies of distribution and abundance of animals.
THE INFLUENCE OF ENVIRONMENT ON TWO SPECIES OF
LAND-SNAILS IN SOUTH AUSTRALIA
by D. E. Pomeror*
[Read 12 October 1967]
SUMMARY
Helicella virgata and IH. neglecta are the most widespread of a number of
species of exotic Jand-snails in South Australia. An analysis of their distribution
and. abundance by multiple linear regressions showed. that the presence of
organic matter in the soil was most important for H, virgata (it could not be
tested for H. neglecta), anc that there wax a strong correlation between the
availability of calcium and the numbers of both species, ‘The availability of
moisture was significant too, but the number of hot days in sammer was markedly
not so. The effects of land use, proximity ta man, and type of vegetation were
of relatively minor importanve, The methad gaye satisfactory results. and might
well be applied to other studies of distribution and abundance of animals.
INTRODUCTION AND METIIODS
The family Helicidae includes several species of snails which have become
established in Australia since the end of the nincteenth century. Of these,
Helicella virgata (da Costa) is now widespread in South Australia, whilst H,
neglecta (Drapamaud), Cochlicella acuta (Miller), C. ventrosa (Ferussac),
Helix aspersa (Miller) and Theba pisana (Miiller) are also abundant in some
localities, and several other species are present in limited areas. Pomeroy and
Laws (1967) described the distribution of these snails in South Australia, and
pointed out that H. virgata and H. neglecta had ranges which were almost
mutually exclusive, and that most of the Jocalities where they occurred were
inside the agricultural areas of the State. They were thus confined to places
having an average annual rainfall of 250 mm or more.
During the summers of 1963-4 and 1964-5, a detailed survey was made of
the distribution of these two species of Helicella on the Adelaide Plains, Mount
Lofty Ranges, Lower and Mid North, Yorke Peninsula and Lower Murray.
Some desert country of the Upper Murray was also included. Snails are easily
seen in summer, when they aestivate conspicuously on fence-posts and similar
places. The margins of paddocks are favourable areas for Helicella, because they
are undisturbed there by cultivation. As most roads are bounded by paddocks
on both sides, roadsides are convenient as well as representative places for Roding
snails. A route was planned which traversed the survey area in a series o
parallel courses at intervals of about eight kilometres. When following this
predetermined route, stops were made at places exactly eight kilometres apart
by road. Tlowever, because the roads were not straight, the sampling-points
could he considered as random with respect to roadside colonies of snails; the
element of randomness is essential ta the statistical analysis which follows.
Qualitative aspects of distribution were discussed hy Pomeroy and Laws
(1967), who publish maps of the distribution of the snails introduced into South
© Department of Zoology. University of Adelaide. Present address; Department of
Forestry and Natural Resources, University of Edinburgh, Seotland,
Trans, Roy, Soc, §. Aust. (1967), Vol. 91.
182 D. k. WYMEROY
Australia. The present paper is concerned with a quantitative analysis of the
results, and their interpretation in terms of the snails’ distribution and abundance.
At each sampling-point, the density of the population of snails was recorded on
an exponential scale, namely:
— if there were none
— if there were less than 2/m?
— if there were between 2.and 20/m"
— if there were between 20 and 200/m2
— if there were more than 200/m*
BwomrS
The decision as to which category was appropriate for a parlivular sampling-
point was made by inspecting at least 20 m bt roadside: (the vhoice as te side of
road being made randomly). Vegetation, aspect, and land-use were recorded
at each of the 415 sampling-points, as well as the numbers of snails (however,
snails were absent from more than half of the places cxaminod).
ASSESSMENT OF ENVIRONMENTAL INFLUENCES
Suitils were mostly absent from places which had native vegetation alongside
the road, but elsewhere there seemed to be little or ne correlation hetween the
numbers of snails and the type of vevetation or crop. However, six other com-
ponents of the snails’ environment were thought likely to be important, and
each could be assessed quantitatively, These six components formed the six
independent varieties in a regression analysis; they were as follows.
(A) Calcium — Many snails are known to be caleiphobes to a greater or
lesser degree, including H, virgata and H. neglecta in their native ranges (Taylor,
1894-1921). The ayailable calcium-content of the soil was therefore one factor
to consider. No direct measurements were made, but the results of detailed
analyses made by the C.S.1.R.0. Division of Soils, and others, were available.
These were studied with respect to measurements of the surface layers of the
suil, the place from which calcium is most likely to be obtained by snails,
Numerical data were not available for all districts, but the caleium-content of
soils tends to be fairly uniform over the whole of the area covered by a particular
type of sail.
Using the map of the soils of South Australia published by Northcote (1960)
together with other analyses, it was possible to estimate the amounts of calcium
in many of the forty or so soils which occur in the survey area. For the remain-
der, 1 was able to call upun Mr. Northcote’s considerable experience, to estimate
the probable calcium-content of those soils for which detailed information was
not available. The result was that for each observation point a rating of 0, 1, 2,
3 or 4 could be given, indicating the probable level of exchangeable-calcium at
that point. (The approximate range of values covered by the ratings is fram
0-2 to 40 mille-equivalents of exchangeable-calcium, per Mg of soil, the ratings
were intended to be linearly arranged within that range.)
(B) Organle matter — H, virguta is primarily a graying animal, and is
dependent on derd and decaying plant material ay its major source of Food
(Pomeroy, 1966). So far as is known, the food requirements of H. neglecta are
similar, The best measure relating to food, and available for the whole area
surveyed, was the amount of organic matter in the soil. The estimated values
for the surtace layers of the soil (where snails feed) ranged from 0 to 4-5%
as measured by the method of Walkley and Black (1984) for organic carbon,
For purposes oF aualysis, these values were reduced to ratings of 0, 1, 2 or 3.
ENVIRONMENT ON TWO SPECIES OF LAND-SNAILS IN 5.A. 183
(C) Temperature — The native ranges of both species of Melivella include
southern Europe, and it seems likely that this was where they originated; but
there are parts of inland South Australia where the temperatures in summer
excved those of Kurope. To test the hypothesis that long periods of high
temperatures might limit the distribution and abundance of Helicella, a variable
known ax “temperature” was defined as the average number of days per year
when the maximum shade temperature exceeded 35°C. Within the area covered
hy the survey deseribed here, the range was from five to forty days,
(D) Moisture — Snails feed only when the surface of the soil is moist.
Sojl moisture is determined by s complex array of factors, but ecologists in
Australia have often found that the ratio of precipitation to evaporation (P/E)
is a useful guide. ‘The number of mouths for which this ratio exceeds 0-3 is
also a measnre of the growing season for plants. Davidson (1935) published a
series of maps, one for each month of the year, showing the places where this
value was exceeded. From these, the number of months when (P/E) was
greater than 0-5 could be calculated for each place viyited. There was a range
of from four to nine.
(E) Land Use — Helicella is rare in native scrub, and uncommen on
permanent pasture. The highest densities seem to be in the well cultivated
districts dominated by the growing of cereals, A hypothesis which would
explain such observations is this: cultivation tends to increase the amounts of
nutrients available at the surface, where they may be directly available to snails,
or may promote conditions favourable to the production of food for snails, As
many of the snails feed in the paddock rather than along the roadside, increasing
cultivation should lead to an increase in the numbers of snails. To test this, the
amount of cultivation was estimated as the probable number of times when the
land would be cultivated in a ten-year period, For example, native scrub and
unimproved pastures both rate as zero, cereal paddocks as three to six (depending
on the area) and market gardens gained the highest rating, fifteen.
(F) Proximity-to-man — Pomeroy and Laws (1967) found that man’s
activities assisted the spread of Helicella in South Australia, in that the snails
were carried along main roads and railways, presumably mostly by agricultural
trafic, Therefore it seemed desirable to discover whether the abundance of
snails at a particular place was related to its distance from the nearest. township,
railway siding, or main road. These distances were measured for cach sampling-
point: they varied from @ to 130 km,
The names and most important propertivs of the varieties to be tested are
summarised in Table 1-
ANALYSIS OF DATA
Multiple linear regressions were chosen as suitable models for the analyses,
each species being treated separately. Not all of the variates were normally
dishibuted, and only variates C, E and F were continuous, but for H, virgety
(where » = 864) both cf these departures are covered, in part at least, by the
central limit theorem. The same applies to #1. neglecta (where n = 51) but
to a lesser extent. The linearity of the independent variates is assumed in the
hypotheses which were being tested. Nome of the independent variates was
highly correlated with any of the others.
Analysis by multiple linear revression yields several useful statistics. Each
independent variate has a corresponding coefficient. whose departure from zero
provides a test of significance. The probability that the regression as a whole
184 D, E, POMEROY
TABLE 1
Summary of the eornponents of the environments of the snails Helicella virgata and H. neglecta
which form the variates for the analysis shown in Table 2.
Variate Unite of Measurement
Dependent yariate; Nu, of snails Arbitrary log-scale: 0, 1, 2, 3, 4
A: Calcium Arbitrary seale: 0, 1, 2, 3, 4
B: Organic matter Arbitrary scale: 0. 1. 2, 3
Independent | C: Tomporature Estimated no. of days/vcar when shade ternpernature
variates above 35°C.
D: Moisture Estimated no, of months/year when P/E exceeded 0-6
E; Land-use Estimated no, of times/10 years when land cultivated
F: Proximity to man| Distance from nearest township, railway-siding, or main
road, in km.
is significant—i.e. that the regression plane is not horizontal—can also be found.
The former test yields the statistic t, and the latter gives the variance ratio F,
The values of these statistics, and the likelihood of them having arisen by chance,
are given in Table 2, It will be noticed that not all of the variates were included
in the final analysis shown in the table. Inclusion of variate B (organic matter)
for H. neglecta was impossible because its rating was constant throughout the
range. Other variates (C for both species, and E for H. virgata) were excluded
because when tested they were clearly non-significant. Their omission increased
the value for the multiple correlation coefficient, R.
TABLE 2
The influence of several factors upon the distribution and abundance of H, virgata and H. neglecta:
results of bwo multiple lincar regressions.
£1. virgala Hf. neglecia
Variate |
Value of t P* Value of t Pe
A. Calcium 2°61 <0-01 2-99 <0-01
B. Organic matter 4-71 <<(-001 — —_—
D. Moisture 2-30 <0-05 1-89 0-05<P<O+1
EK, Land-use - ae 1-46 hl oPooe?
FP. Proximity-to-man 1-88 0-08<P<t)-1 0-937 3 <P<0-4
| a
Test of regression as a whole F j4sa6a) = 9-173 | F taj4g) 3746;
P< <0-001 P=<0-02
*Probability of calculated value arising by chance alono,
tNegative coethicient,
DISCUSSION
-
There was a close relationship between the numbers of H. virgata and the
amount of organic matter in the soil. This agrees with the observation that
snails feed upon organic detritus, and probably upon the micro-organisms which
are themselves feeding upon the detritus (Pomeroy, 1966). The degree of
ENVIRONMENT ON TWO SPECIES OF LAND-SNAILS IN 5.4, 185
statistical significance associated with this factor is high, and it was particularly
disappointing 10 be unable to make a comparable test for H. neglecta.
For both species, density was highly correlated with the amount of calcium.
This is almost certainly because uf its importance in the shell, which accounts
for about one quarter of the weight of a helicid snail; and about 98% of the weight
of the shell is calcium carbonate (Pelseneer, 1935). Inability to obtain sufficient
calcium affects the structure of the shell, which may become extremely fragile,
thus reducing its efficiency as a skeletal structure.
Next in order of significance was soil moisture, It was emphasized pre-
viously that this is hard to measure. and the achievement of a significant result
could be explained in several ways. The amount of rain, number of wet days,
number of wet nights (including those with dew), and measures of the tendency
of the soi] to dry, all will be correlated to some extent with measurements of
P/E; the exact extent of the correlation itself depending upon complex facters,
some general and some local. [t can only be concluded that some aspect or
aspects of soil moisture are important, and are reflected in the measurement of
P/E, However, it is known that availability of water limits the time when
Sale at be active, in addition to its nevessity ta the organisms which constitute
their food,
Proximity-to-man seemed to be important in determining the abundance of
H. virgata, thus supporting the hypothesis being tested. A more significant
result would probably have been obtained if this factor had been tested only
for the more remote parts of the survey area; closer to Adelaide, where the
species has heen established for several decades. it has lad longer to reach all
the suitable places. In any case, this variate could mot exceed a value of two
within 50 km of Adelaide. because of the relatively high density of human
occupation, By contrast, the much less significant result for this variate for
H. neglecta is rather interesting, Southern Yorke Peninsula, where it occurs,
is rather sparsely inhabited, and the mean value for the variate was T'S km
(as compared with 3-0 for Hf. eirgata). There is some eviclence that H- neglecta
has been established on Yorke Peninsula for many years (Pomeroy and Laws,
1967), so that it may have reached its maxinmun distribution, at least for present
eoditions, throughuut its range. Considered in this way, the variate “Proximity-
to-man” becomes a measure of the present tendency to spread; a high score
indicates rather recent arrival, and snygests that futuro enlargenient of the
range is likely.
Numbers appear to be weakly correlated with land-use in the case of JT,
neglecta. For H. virgata there is no support for the hypothesis that increasing,
Jand-usc makes the environment more favourable, It is possible that further
investigation would yield q different result, as this variate (if it is important) is
the least likely to be linearly related to y: too much cultivation could be as
unfavourable as foo little, in that snails wonld be physically damaged, or become
buried.
The absence of any correlation between the distribution and abundanoc of
snails and the number of hot days is also interesting. It is consistent with the
conclusion that Helicellu is remarkably resistant to the effects of high tempera-
tures. It was found that when the screen temperature is 33°C, even for a short
time, the internal temperatures of snails often exceed 40°C (Pomeroy, 1966),
And, within the survey area, there were many places where the screen tempera-
ture was estimated to exceed 35°C. on more than thirty days a year; snails were
present at many of these places.
186 D, E. POMEROY
In so far as comparisons between the two species arc possible, the results
for H. virgata and H. neglecta are closely similar, suggesting that their Tequire-
ments are similar too. Perhaps this is to he expected for congeners, since closely
related species usually have similar feeding preferences. It might offer a partial
explanation of the observation that the distributions of the two species in South
Australia are mutually exclusive, or nearly so.
Whilst it is useful to have obtained some objective support for several
hypotheses about distribution and abundance, it must be stressed that the
analyses only accounted fora small proportion (less than a quarter) of the total
variance. This can mostly be explained by the poor quality of much of the
data, but a possibility that cannot be excluded is that one or more important
variates escaped notice altogether. The method seems to have been satisfactory
in other respects, and could probably be applied to many other situations. The
precision of the results obtained from such a suryey would depend upon the
correct choice of variables, and the accuracy of measurement.
ACKNOWLEDGMENTS
The author expresses his thanks to Professor H. G. Andrewartha of the
University of Adelaide for adyice during the work, and for kindly criticizing
the first draft of this paper. Professor J, N. Black and Dr. D. Mills also read
the manuscript, and made useful comments on it. Myr. K. H. Northcote, of the
C.8.LK.Q, Division of Soils, helped me to interpret the soil analyses for South
Australia. The unpublished data for temperatures in South Australia were
provided by the Bureau of Meteorology, Adelaide, and Mr. B. Mason of the
University of Adelaide helped me to compile a map from them.
REFERENCES
Davmson, J,, 1935. Climate in relation to insect ecology in Australia. 2: Mean monthly
PaaS and. precipitation-cvaporation ration, Trans, Roy, Sov. S. Aust, 59, pp.
07-12
Norrucote. K. H., 1960, “Atlas of Australian Soil; 1, Pt, Augusta-Adelaide-Hamilton Area.”
C.S...R.0., Melbourne, _
PerstNeer, P,, 1935. “Essai d’lithologie Zoologique d'apréy l'étude des Mollusques.” Acad.
Roy. Belg., Brussels. ]
Pomrnoy, D. E., 1966. The ecology of Helicella virgata and related species of snails in South
Australia, Ph.D. thesis, University of Adelaide.
Pomeroy. D, E,, and Laws, Hetene M.. 1967, The Distribution of Introduced Snails in
South Australia. Rec. 8. Aust. Mus., 15, No. 3 (in press).
Tarxcor, J. We eee Teak: “Monogiaph of the Land and Freshwater Mollusca of the British
Isles,” Lecds.
Wark.ey. A,, and Bracw, ft. A. 1934, An examination of the Degtjaress method for deter-
ming soil organic matter, aucl a propused modification of the chromic acid titration
method. Soil Sci., 87, pp. 29-38.
MICROHYLID FROGS OF NEW BRITAIN
BY MICHAEL J. TYLER*
Summary
The morphological characteristics of the two species of microhylid frogs occurring in New Britain
are reported. Oreophryne brachypus was last collected seventy years ago, whilst Sphenophryne
mehelyi represents an addition to the fauna of the island. The latter species was found in
aggregations estimated to reach 300 specimens, and the females sit on clumps of up to six eggs in
depressions beneath rotting vegetation.
MICROHYLID FROGS OF NEW BRITAIN
by Miciuar. J. Tyier*
[Read 12 October 1967]
SUMMARY
The morphological characteristics of the two species of microhylid frogs
occurring in New Britain are reported. Oreophryne hbrachypus was last col-
lected seventy years ago, whilst Sphenophryne mehelyi represents an addition
to the fauna of the island. The latter species was found in aggregations esti-
mated to reach 300 specimens, and the females sit on clumps of up to six eggs
in depressions beneath rotting vegetation.
INTRODUCTION
The only microhylid frogs reported. from New Britain are the three syntypes
of Oreophryne brachypus (Werner) collected in 1897. In the course of a visit
to the island im January-February, 1966, the writer collected a series of speci-
mens of this species. Later in the same year Mr. D, Morgan of Keravat on the
Gazelle Peninsula collected further specimens and also large numbers of Spheno-
phryne mehelyi Parker, a species previously known from the two types collected
in New Guinea,
The present contribution records morphological variation and field observya-
tions on the two specics. The methods of measurement employed in the text
conform to the techniques of Zweifel (1962).
Oreophryne brachypus (Werner )
Material Examined: 22 specimens—South Australian Museum, R.6910, 6942.
6044, 6948, 6964. 6989, 7025, 7065, Pomugu near Kandrian, South New Britain;
6992, G99T, TO. 7002, 7004-5. 7008, Aliwoh near Katidrian; 7749, 8123, $440
(5 specimens), Keravat, Gazelle Peninsula. ’
Variation: The series consists of sixteen adult males, three adult females and
three juveniles. The ranges and means of the snout to vent lengths of the adults
are as follows: males 19-2-22°3 mm (mean 19-9 mm), females 21-5-22-8 mm
(mean 22-0 mm). The syntvpes are two adult males and a juvenile and each
male has a snout to vert length of 21-3 mm.
These specimens conform closely to Tyler's (19635) redescription of the
species; the only additional information relates to the colour of the species. In
life brachypus has a dusky brown ground colouration with indistinct and slightly
darker markings upon it. Of these markings the most common are a narrow
trans-ocular bar and a W-shaped patch immediately behind the head, There
bas been nu visible change after a period of fifteen months preservation.
> South Australian Museum. North Terrace, Adelaide, South Australia.
Trans, Roy. Soc. $, Aust, (1967), Vol. 9b
188 MICHAEL J, TYLIER
Field Notes: The males were located at each locality calling from vegeta-
tion at heights of from three to eight feet fiom the level of the ground. ‘The call
consisted of a single note, resembled a long squeak and had a duration of about
four seconds,
Sphenophryne mehelyi Parker
When Parker (1934) described this species the only specimens availahle to
him were two on Joan from the museum at Budapest which he designated type
und paratype respectively, The specimens hal been reported previously (as
Chaperina fusca) by Méhely (1901), ‘Che herpetological collection at Budapest
was destroyed in 1956 and there are na known lopotypie specimens in existence,
The specimens referred here to mehelyi agree in alinost all xespects with
Parker's description and there is pertect agreement with the reported colouration
of the type which, to judge from comparisons with species in the South Aus-
tralian, Museum collection and descriptions in the literature, is quite unlike
that of any other species of Sphenophryne.
It is pertinent to note that the type locality (Sattelberg) is located on the
Huon Peninsula, the portion of New Guinea in closest proximity Lo New
Britain.
Material Examined: 857 speeimens—Seuth Australian Muse 28.7785-7839,
7955-500U, 8186 (232 specimens), 6438 (15 specimens), Keravat Corrective
Institulion, Keravat, Gazelle Peninsula,
Variation and Comparison with Original Deseription; Of the above. speei-
ments a series of 55 (.7785-7839) have heen examined in detail amd measured.
Nineteen proved to be adult males, 27 adult females (of which 21 were gravid)
and @ sexually immature specimens, The ranges and means of snout to vent
lengths of the adnits were as follows: males 15°5-17-2 mm (mean 16:3 mm),
femules 17-0-20-1 min (new 18-7 nn),
Parker's figure of 20 mim as the size of the holotype was not the snout to vent
length. Me states in an adeaunt of his descriptive methods Mist, p. 16), “The
length of a frog, is the maximum distance in a straight line between the tip of
the snout and the hinder side of the thighs behind the vent.” This “total length”
would exceed the snout to vent length by about one millimetre, placing the size
of the holotype very close to the mean snout to vent Jength of the females vx-
amined, As noted by Zweifel (1962), Méhely (1901) cites a figure of 24-3 mm
for the same specimen and, since it is highly probable that his measurement
is the “total length” m vogue at that time, this would indicate a snout to vent
lenwth of ahout 23 mm,
‘Vhe specimens tally with Parker's original deseription in the following
respects; the presence of a denticulated prepharyngeal ridge with an adjacent
median swelling; the distance between the eyé and the tip of the snout is approxt-
nately equal to the horizontal diameter of the eye; the loreal region iy oblique;
the nostrils are nearer the tip of the snout than the eye; the interorbital space
is equivalent to twice the diameter of the upper cyelid; the fingers are short
and equipped with small dises; the toe dises are larger than the finger discs:
wher the hindlimb is adpressed along the side of the body the kuee reaches
the eye. The colouration of the present specimens agrees in all respects with
that of the holotype.
The canthus rostralis of mehelyi is said to be rounded but most of the
Keravat specimens exhibit only the slightest curvature and in some it is definitely
straight. A further point of divergence concerns the length of the fourth finger.
MICROHYLID FROGS OF NEW RRITAIN 18S
Parker reports that in the holotype it is equivalent to iliree-quarters of the inter
narial span, whereas its length exceeds the internarial span in the present
material, ‘The tympanum is said to be distinct and, “rather less than half the
diameter of the ‘eve’. This is truc of the majorily of specimens, but in those
in which the skin on the side of the head is at all loose, the site of the tympanum
cannot be detected externally, The skin appears stnouth when superficially
examined, but minute tubercles ure visible when it is examined beneath the
inicroscope.
In Parker's key to Sphenophryne the tibia of mehelyi is said to equal ahout
half the distance from snout to vent, and to reach the couplet containing mehelyi
involves agreement with, “tibio-tarsal articulation reaching the cye’. As indi-
cated in a previous paragraph, the knee of the adpressed hind limb of the
picsestt material will reach the eye, but the tibia length is consistently less than
1alf of the snout to vent length, A frog whose tibia Jength is exactly half the
snout to vent length has a TL/S-V ratio of 0:500, whereas the range of the
jwesent material is +354--432,
The significance of these points of divergence from the original description
caunot be determined until adequate topetypic material is available. At the
present time it is considered that the interests of nomenclatural stability are
best served by regarding the New Guinea and New Britain populations. von-
specific.
Comparison with Other Species: Of the thirteen species currently recognised
five have snout to vent lengths exceeding 34 mm (curnuta, macrorhyncha,
palmipes, rhodadactyla and schlaginhaufeni), The maximum recorded size uf
the present material (20-1 mm) therefore prevents any confusion with these
SPECIES,
Sphenophryne hrevicrus, brevipes, and crassa lack dilated discs on the
fingers (present in mehelyi) whilst polysticta has a bluntcr snout, shorter hind-
limbs and a different colouration,
Of the three Australian species reported hy Zweifel (1962, 1965), 5. fryi
has shorter limbs (TIL/S-V 0:31-0:38, mean 0-346, as opposed to 0-35-0-43,
mean 0-390) and attains a larger size than mehelyi (of more than 25 specimens
reported by Zweifel (1962), only one adult had a snout to vent length of Jess
than 20 mm, whereas 20-1 mm is the maximum tor mehelyt). Sphenophryne
plunlalis is evidently also a larger species than mehelyli and the specimens re-
ported by Zweifel were uniform in hearing, “ill-defined, and irregitlar dark brown
spots”, on the dorsal surface of the body. There is no trace of any dorsal mark-
ings on any of the 337 mehelyi.
The size and TL/S-V ranges of robusta are similar to those of mehely: bunt
the reported colouration of the former (although variable) is evidently quite
distinct from that of mefhelyi. :
Ficlil Notes: Vhe specimens were found congregating bencath piles of
decamposing vegetation, consisting of rotting grass and reeds laid upon ground
covered with leaf mould, The piles covered arcas of up to five square yards, As
many as 250-300 mehelyi were estimated to occur together but, when the yege-
tation was removed the frogs rapidly dispersed in all directions and rarely were
more than 50 or 60 captured ut any one site.
Numerous females were found at the base of the piles sitting upon clumps
of eggs at the fout of small depressions excavated to a depth of about two inches
in the leaf mould. Each egg clump consisted of five or six eggs connected to one
190 MICHAEL J. TYLER
another (in the form of a bead necklace) by a very fine cord. Subsequent
measurements of the eggs revealed a mean diameter of 3-3 mm for those at a
stage prior to gastrulation, and 4-8 mm for those containing well developed
juvenile froglets apparently near to emergence. Six eggs is virtually the maximum
number that a female of this diminutive species could cover with her body.
Three months prior to the collection of the frogs the area in which they
were found was virgin rain forest, but subsequent deforestation had completely
eliminated the natural environment of the species. It therefore remains un-
certain whether the aggregation of large numbers of frogs in breeding condition
is a natural phenomenon, or simply necessitated at Keravat by the reduction
in the amount of rotting vegetation occurring in the area.
REFERENCES
Menery, L. (1901), Beitrige zur kenntniss der Engystomatiden von Neu-Guinea,
Termesz. Fiz. 24, pp. 169-271.
Parker, 11, W. (1934). A monograph of the frogs of the family Microhylidae. London,
British Museum (Natural History), viii + 208 pp.
Tyten, M, J. (1965), Transfer of the New Britain frog Hyla brachypus (Werner) to the
microhylid genus Oreophryne. Mitt. Zool. Mus. Berlin, 40 (1), pp. 3-8.
Zweiret, R. G, (1962), A Systematic Review of the Microhylid Frogs of Australia. Amer.
Mus. Novit., No. 2113, pp. 1-40,
Zweiret, R. G. (1965), Revisionary Notes on Australian Microhylid Frogs of the Genus
Sphenophryne. Ibid., No. 2214, pp. 1-9.
A NEW SPECIES OF FROG OF THE HYLID GENUS NYCTIMYSTES
FROM THE HIGHLANDS OF NEW GUINEA
BY MICHAEL J. TYLER*
Summary
A new species of Nyctimystes is described. The maximum recorded snout to vent length of males is
more than 80 mm, and the species shows distinct affinities with N. humeralis (Boulenger).
However, it lacks the characteristic humeral spine exhibited by males of that species, and is also
distinguished by its undivided nuptial pad and by differences in colouration.
A NEW SPECIES OF FROG OF THE HYLID GENUS NYCTIMYSTES
FROM THE HIGHLANDS OF NEW GUINEA
by Micmac. J. Tycer*
[Read 12 October 1967]
SUMMARY
A new species of Nyctimystes is described. The maximum recorded snout
ta vent length of males is more than 80 mm, and the species shows distinct
affinities with N. humeralis (Boulenger). However, it lacks the characteristic
bumeral spine exhibited by males of that species, and is also distinguished by its
undivided nuptial pad and by differences in colouration.
INTRODUCTION
In 1963 and 1964 Mr. Barry Craig donated to the South Australian Museum
several large collections of frogs obtained in the vicinity of Telefomen in the
Western Highlands of New Guinea. Amongst the specimens were eleven
representatives of an undescribed species of the hylid genus Nyctimystes. In
1965. Mr. Craig was a member of the Australian Star Mountains Expedition
and obtained 650 frogs in an area approximately 40 miles west of Telefomen.
Included in the collection were four additional specimens of the same specics.
The methods of measurement employed in the description of the new
species conform to those used by Tyler (1963).
Nyctimystes zweifeli new species
Holotype: South Anstralian Museum R.5426. An adult male collected at
Telefomen, Western Highlands, New Guinea, on November 24th, 1963, by
B. Craig.
Definition: A particularly large specics of Nyctimystes in which males have
a snout to vent length of up to 83 mm, The hindlegs are very long with a tibia
Jength to snout to vent length ratio (TL/S-V) of -588--654. The veins of the
palpebral venation are largely vertical in their vrientation with a tendency to
form a reticulum.
Description of Holotype: The vomerine teeth are in two roughly oval and
promincnily raised series between the oval choanae. The tongue is less than
half as wide as the mouth, oval in shape and with a very slight posterior inden-
tation. The head is broader than long (head length 26-8 mm, head width
29-4 min), The snout is. blintly rounded when viewed from above and strongly
rounded in profile. The canthus rostralis is slightly curved and the loreal region
oblique. The nostrils are inconspicuous and separated from one another by a
distance which is slightly less than the distance between the naris and the eye
(eve to naris distance 7-2 mm, internarial span 7-0 mm). The eye is relatively
small and not prominent, its diameter (7-8 mm) only slightly greater than
* South Australian Moseum, North Terrace. Adelaide, South Australia.
Trans. Roy, Soc. S. Aust, (1967), Vol. 91.
192 MICHAEL J. TYLER
the eye to naris distance, The pupil is completely dilated. The jalpebral
venation forms a dense pattern of predominantly vertical lines. The tympanum
is small (diameter 3:7 mm) with only the inferior portion of its annulus visible.
The distance from the snout to the vent is 75-9 inm.
The fingers are long with large terminal discs, broad lateral flanges and
llattened subarticular tubercles (Fig. la). The webbiny between the third and
fourth fingers reaches the base of the subarticular tubercle heneath the peuulti-
mate phalanx on the third, and midway up this tubercle on the fourth, Fingers
in decreasing order of length, 3, 4, 2,1. The dises of the second, third and
fourth fingers are larger than the tympanum.
The toes are almost fully webbed, the webbing reaching the dises of all
toes except the fourth where it extends as far as Ue subarticular tubercle at the
base of the penultimate phalanx, and continues to the disc as a broad lateral
flange (Fig. 1b). The toe discs are only slightly smaller than the finger discs,
and ull are larger than the diameter of the tympanum, There is a small kidney-
shaped inner but no outer metatarsal tubercle. The legs are extremely long; the
tibia length is 47-4 mm and the tibia length to snout to veut length ratio
(TL/S-V) is 0-625. When the hindley is adpressed the heel reaches well
beyond the tip of the snout; when the hindlegs are laid alony the side of the
body the knee and elbow overlap considerably; when the hindlegs are bent at
right angles fo the axis of the body the heels overlap slivhtly.
The skin covering the dorsal surfaces of the head, body and limbs is smoath.
The lateral surfaces of the body are slightly granular, the throat and chest finely
granular and the abdomen and undersurface of the thighs coarsely granular.
There is an oxtremely prominent supratympanic fold, a sharp fold on the
posterior surface of the tocearm, and a less conspicuous tarsal faldl,
The dorsal surfaces of the head, body, forearms and tibia are a very dark
Plum colour with. a hint of a crimson suffusion on the dorso-lateral portion of
the body. On the thighs the plum occupies the median portian whilst the
anterior and posterior surfaces are white, Jeavily suffused with large, regular
spots of plum. The sides of the body, the tarsus and foot are similarly marked.
The abdomen is ercam and the vemainder of the ventral surfaces grey witli
obscure brownish mottling,
There is a sub-gulay vocal sac with paired openings in the Aoor of the muuth
near the angles of (he jaws, and an extremely large, black nuptial pad at the
hase of the first finger.
Variation: There are eight paratypes: South Australian Museum R.SSL2
881) collected at the type locality during the period November 14th-18th, 1983,
by B, Craig. All specimens are males (six adults and two juveniles), Six addi
tional male specimens from other localities are clearly representatives of N,
sweifeli; South Australian Museum R.5275, $811, Okfekarnan, approximately 10
miles west-north-west of Telefomen; R.6476, 6499, Kawolabib (141°O5’ lonw,,
5°08" lat.), approximately 10 miles south-east of Capella, Star Mountains; 8.6477,
Begibajen near Kawolabib and R.6478, Tabek Creek, Kawolabib. The complete
range of allitude of these localilies is 4,700-5,500 ft.
The range of snout to vent length of the arlult males is 60-8-83-4 mm, but
the smallest specimen with a ouplial pad (8.8815) measures 73-6 mm.
There is very little variation in the proportions of the coniplete series. In
one specimen the internarial span is equal to the eye to nariy distance, and iss
the remainder slightly less than it, the eye to naris to internarial span ratio
HYLID GENUS NYCTIMYSTES FROM THE HIGHLANDS OF NEW CUINEA 193
14 MICHAEL J. ‘TYLER
{E-N/IN) being 1:000-1-12] with a mean of 1-063. This is an exceptionally
long-legged species, for the 'T1./S-V range is °588-'654, with a mean of -625.
The supratympanic fold is conspicueus in all specimens, whilst the fold of
skin on the posterior surface of the forearm of two shows a tendency to form
tubereles. In the remainder it is a continuaus fold as found in the holotype.
Finger webbing and the palpebral venation are features in which there is scant
variation. (Four examples of the palpebral venation are depicted in Fig. Ic, )
The dorsal colouration varies from a very dark plum to pale violet. In the
darkest specimens patehes of dark slate are visible. Ina few specimens there are
a few tiny, brilliant white rings scattered on the dorsal surface, Markings on
the thighs appear to increase in intensity with age. In the largest specimens
the pale background of the anterior and posterior surfaces is almost completely
obseured by irregular patches of plum and slate. There appears to be a similar
correlation with markings on the ventral surface of the body, for in juveniles
and small males it is an immaculate pale cream. In three specimens there are
no islands of pigmentation on the lateral bedy surfaces vr on the anterior and
posterior surfaces of the thighs.
The size and number of the spines which make up the nuptial pad vary with
the size of the individual, In the largest males the spines are larger and less
numerous than in the smaller specimens.
Comparison with Other Species; The large size of sweifeli clearly distin-
quishes it from all species except granti, humeralis, kubori, montana, naritiose,
papua, perlmeiri and pulehra. (The species referred to here as N. montana
is montana (Peters and Doria) and not the species described by Parker, 1936,
for which the substitute name cheesmant wis proposed by Tyler, 1965.)
The only specimen of granti reported in the literature is the holotype female
with a length of 100 mm. A female specimen from Antares (Rijksmuseum Van
Natunrlijke Historic, Leiden, No, 12110) approximately 250 milus cast of the
type locality has been examined by the writer, It is a female with a snont tu
vent Jength of 70 mm; it agrees with the original description of Boulenger (1914)
and perfectly reproduces the striking vermiculated pattern of the dorsul surface
seen in the illustration accompanying it. From a comparison of this specimen
with <weifell, granti may be distinguished by its shorter legs (TL/S-V +537).
more widely spaced nares (E-N/IN +790), less extensive finger webbing (nal
reaching the subarticular tubercle at the base of the penultimate phalanx of the
fomth finger), and by its entirely different dorsal colouration,
The largest male knbori reported in the literature had a snout to vent length
ot 53. mm which is less than that of the smallest elias (60-Simm). Further
more, the possession of a definitely reticulate and more heavily piemented
palpebral venation, and shorter limbs (TL/S-V 0:51-0:57, vide Zweifel, 1958)
enable kubori to be readily distinguished from suweifeli.
In montana the eye to naris distance is considerably greater than the inter-
narial span (only slightly less than the internarial Spas in aineifeli), the finger
webbing is slightly more extensive and the palpebral venation is cumposed
solely of vertical lines. Nyctimystes narinosa has an internarial span exceeding
the eve to naris distance and only basally webbed finuers. In papna the legs
ave shorter than those of 2weifeli (TL/S-V 0-5L-0-58), the fingers are less
extensively webbed und the palpebral venation is bruken up inta isolated
segments,
HYLID GENUS NYCTIMYSTES FROM THE HIGHLANDS OF NEW GUINEA 195
Nyctimystes perimetri has a high E-N/IN ratio (1-20-1-39 compared with
1:00-1:12 in zweifeli) and short legs (TL/S-V 0:50-0:56), whilst pulchra
possesses a slightly crenate ridge on the forearm and tarsus and a long heel
lappet (zweifeli lacks these dermal appendages ).
Nyctimystes humeralis has a similar size and similar proportions to those
of zweifeli and shares in preservative a violet dorsal colouration. The former
is distinguished in being immaculate and in the sexual characteristics of male
specimens. Male humeralis possess the unique humeral spine and there are
two separate nuptial pads at the base of the first finger. Male zweifeli lack a
humeral spine and the nuptial pad is undivided.
Colloguial Nomenclature: All of the specimens from Telefomen and Okfe-
kaman were referred to as “Itul”,
REFERENCES
Boutencer, G. A. (1914). An annotated list of the batrachians and reptiles collected by the
British Ornithologists’ Union Expedition and the Wollaston Expedition in Dutch New
Guinea. Trans. zool. Soc. London, 20, pp. 247-274,
Parker, H, W. (1936). A collection of reptiles and amphibians from the mountains of
British New Guinea. Ann. Mag. nat. Hist., ser. 10, 17, pp. 66-93,
Tyxen, M. J. (1963). A taxonomic study of amphibians and reptiles ofthe Central Highlands
of New Guinea, with notes on their ecology and biology. II. ANURA: Ranidae and
Hylidae. Trans. Roy. Soc. 8. Aust., 86, pp. 105-130.
Tyzuer, M, J. (1965), An investigation of the systematic position and synonymy of Hyla
Regnor Peters and Doria (ANURA, Hylidae). Zool, Abh. Dresden, 27 (10), pp.
Zweiret, R. G. (1958). Results of the Archbold Expeditions. No. 78 Frogs of the Papuan
Hylid Genus Nyctimystes. Amer. Mus. Novit., No. 1896, pp. 1-51.
OBITUARY:
DR. P. S. HOSSFELD
Summary
197
OBITUARY
Dr. P. S. Hossrenp
Paul Sanyirel Hossfeld died in Adelaidy on the 15th Joly, 1967, at the age of Tl. His
education commenced at Dutton, where he was barn. und wus continued ut Prince Alfred
College, He devoted some years to teaching before entering the University of Adelaide as
a science student. He graduated as B.Sc, in geology and chemistry in 1924. and as M.Sc. in
1926. He was then appointed assistant to Dy. W. G. Woolnough, Geological Advisor to the
Commonwealth Government. In New Guinea in 1929 he disenvered. near Aitape, part of a
hainan skull} in beds of apparently late Pleistocene age. In 1935 he was appointed Jeader
of » section of the Aerial. Geological and Geophysics) Survey of Northern Australia and this
gave him a wide knowledge ot the geology of the Northern Territory. This work was <lis-
rupted by the war, during which Hassteld worked as an industrial chemist. Later, he
returned to the University and was awarded the degree of Ph.D. in 1953, He was appointer]
Lecturer i the Department of Geology and Mineralogy in 154 and Senior Lecturer in 1Y3Y,
Among Hassfeld’s varied vontributions to. geology, three are pasticularly notable, In his
early detailed work in the northern Mount Lofty Ranges be advocated subdivision oF thr
rocks of the Adelaide System into two serics. the lower of which, the Para Series, corresponds
clusely with what, many years later, was named the Torrensian Series. the priority of Fass-
feels work and term apparently being overlooked, Probubly his best known work is thal
on the stratigraphy of the Northern Yerritory, Tis is un immense compilation and the result
af many years work: Elis contrihbation to the Cainozoic History of the South-east of South
Australia overlapped two of his great interests. Quaternary geology and the study of alsariginal
man, which, in later years, received much of his interest, ‘
All Hassfeld’s work was characterised by intensity of effort. It was typival af him that
in 1962, at the age of 66. he walked greut distances through New Guinea jimgle to obtain
materials which would give a radio-carbon dating of the skull fragments he had fovnel at
Ajitape thirty-seven years earlier, Paul Hossfeld was a dedicated teacher and far this earned
many tributes from both callengues and students, "
ALHLA,
SELECTED BIBLIOGRAPHY
1925. Tas Teen Creek Granite and its Field Relations, Trans A, Sov. S. Aust, 44, pp.
(91-197,
1926 (With D. Mawson): Relies of Aboriginal Occupation of the Olary District, Trans BR,
Soc. S. Aust., 50. pp. 17-24.
1928 The Aborigines of South Australia; Native Occupation of the Eden Valley and Angus-
ton Districts, ‘Trans. R. Soc, S.. Aust., 50, pp, 287-297,
1935 the Castny of Part of the North Mount Lofty Ranges. Trans. BR. Sov. S. Aust 5°,
pp. 16-67.
1936-1941 Twentytwo reports on the geology of the Noithern Territory published! by the
Aerial] Guol. & Geophys. Sury, N, Aust,
1946 (With T. D. Campbell und J. B, Cleland): Aborigines af the Lower South-vxst at
South Australia, Ree, S. Aust Mus. 8 No, 3. pp. 445-501. ;
1949 The Stratigraphy of the Aitupe Skull and its Signifleance. Trans. R, Sos, S, Aust.
72(2). pp. 201-207,
149 The Significance of the Occurrence of Fossil Fruity in the Barossa Senkungsfeld, Sputh
Australia, Trans. R. Soo. S. Aust., 7T2(2), pp. 252-258,
1950) The Late Cainozoie: Mistory of the Sonth-east of South Australia, Trans. R. Sov. S.
Aust., 73(9). pp. 232-279.
1954 Stratigraphy and Structure of the Norther Territory of Australig. Trans, B, Soc, 4.
Aust, 77, pp, 108-161,
1964. The Aitape Calvarium. Aust. J. Sei, 27(6), p, 179.
1964 Tadioeearhon Dating and Palaconvology of the Aitape Tossil Murnan Remains, Pres.
R, Sac. Viet., 7T8(2), pp. 161-165,
1965 (With 'T. D. Campbell): Aboriginal Stone Circles. Mankind 6, No. 4, pp, 181-183.
1966 (With T, DB, Campbell): Australian Aboriginal Stone Arranvements in North-east
South Australia, Trans, R. Soc, S. Aust, 90. pp, L71-176.
1986. Antiquity of Man in Australia, Pub. in “Aboriginal Man in Santh and Central Aus
tralia”, Government Printer, Adelaide. pp. 59-95,
1966 Mutorialy Used in Australian Aboriginal Stone’ Tinplements. Pub: in “Alsoriging) Maa
in South und Central Australia”. Govermnent Printer, Adelaide, pp. 163-168.
BALANCE SHEETS:
GENERAL ACCOUNT AND RESEARCH FUND
Summary
198
Fr ESE ee FF 1833S
Soria " LOGT “9unf Mog w I aouryeg Brrso[D
ea es 4 sarpung
eO'6IT aouBInsuy
O0'8L6 Aurpurg
00'FOS 7 880) TBOUs[D SP Sr ~ “ asaroUy Aue
PL Ele sageAy Ss Wermrerqry FG6'SSET ~~ guonoRsaely, JO ales
OC LTE syuriday uosuyol SO'COF'T a96t ‘Aun Sf Ie souveg surradg
$ $
SLINGWAVE SLdIS0a
L961 “ANOL oe GAUNA UVAA AHL YOA SLNAWAVd GNV SLdId0aH JO LNANALYLS
INQNODDY AuVusIT
Be PL0'9s SS FL0'D$
96°L02 _ a = = L9GT ‘aunf TIOEg F se sourfeg Suyso[D
28°06 . z - “ . Soprpuns
gf 6FE “2 = = ao qUNOAdDY Yomasay O} Iazsuery,
0S'0F "3 ve om - “ AosBey Ayodorg pue Koy
GL TIL ry i “4 I Ba ~<a ™ Sa0ljON jo sugung PL SP ? 7 7 7 , thd aumooUuy Arpung
00'FT re HY fa es “ aa id ie suLOOY JO WI Ont bes oe na * _t ot - ysaraquy puog pue Yaeg
So Or ad au “re bot Si v _ ~ sasivyy BITAIOS 00°009 _ - vr a a * ~ ApIsqns | BN SsUy ATTRA
G6'S8T a a K ns . ™ p w ysesy Aneg 00°96F x a x sunday
G6'691 “ i a id “ adeysog oo';ooL’e si rr “ “ e yoeig yuauTUIeAOs
00°9ST Sal . ‘i sysoF) Burtuayy £o'SSo'T - mm suogdrosqns
6es0Cr * ba C sso Surysiqng é8'69L 996t “anf WT We aouejeg RuruedD
$ $
SINGAAVd
SLdI FOR
LOGI “ANOS oe GHANA UVHEA AHL HO4 SLNAWAVd GNV SLdIHOeH AO LNAWALVLS
LNNOODY ‘IWHANAL)
CGHYLVYOdUOONI VITIVULSAV HLNOS AO ALHIOOS 'IVAOU AHL
199
gquuejunosy paeHneyy
“OD ® ADUVAS “SNEAALS ‘ANTIW *LOGT “Iaquiajdag jo yc
‘eyjeasny weg ‘apreppy
“LOGT “aunf YyIOE yw syWauysaauy JO ayNpayOs wyy payed os[e advYy aAq "pazruIqus AyaID0g aly yo syoog ayy Aq uMos se
pues sl Of WaAIT suOKeURIdxD ayy PUB UONEUIOFUT INO FO seq oY} 03 BuTprcOoR ‘29qG)] ‘ounf WOE Pepue iwak ay AOF AJataog ayy JO suoroRsuex Ysa ayy
piooar 0} dn umeip ATE oid are puny yWauimopug pus Areiqry ‘ferauay) ayy AOF SyuewAET pur s}dianay Jo SWauraqyeyg peyovye ayy ‘uorurdoe ma ut
‘palmbex aarey am suotjeurjdxa pues woyeUtosuT 343 [[e pouteiqo osvy pue ‘p96, ‘aunf Mog papuo
weak ayy 10} ((ALVHOdYOOND) VITIVULSOY HINOS dO ALAIOOS 'IVAOH AHL J Syunod0y pur syoog ay} peuluxa savy am yeyy HOder aA,
iuoday SvoLlaay
OO'RLTOG$
00'PES i = he 7 tw vs “ yueg 1B Yyseg
00°008, +e be + i “ (js09 38) YPo}s poqiasuy
OOF = —~—-— (LOS‘OTS ‘anteA JeyLW)
oooss tT Be Be - ? OSé—"PIT Sqo],
ooLgeT a “ OOe—SeUTL AppsA, pus presi
oosea tT % "u ‘4 ny ~ 00F—"W'S'D
OSL T +7 7 ~ O08—wsuts spre[epy
OOLsTT es “ ty a a 00F-TI¥
OO°SLP'T ; “ a 4 - a 008d’ H's
OOOb6ST - al 7 , 0OG—StPAOMOO AA,
(3809 Je) yxpo3g Aymby
00°006°6 = —--—— ;
00°006_ is 7 ' ~ 7 = %8—" TEA
00000" a . . ‘ e 6EL—VWO's
oo°;o0o TL ~ % ~ , %9I- DV WO
00°000 6 %EL—OVW'OD
OO D00'FS 7 — 7 %e-saueuLy YOMsuaT
—(1s09 ye) sytsodaqy paxryt
$
A961 ‘ANO{ n0¢e L¥ SV SLNANLSAANI JO 37TAIdgHOS
LVFSS' TS LUFESTS
88'6ES *¥ 7 ‘ ‘. ~ ~ ynnowy ]erauas) wloiy rozsuviy,
ZO'ET a 40 “ jes ws ‘ ff a qsaisquy yueg
LUPES a hg _ ” LOGI “AUNf TOG 4 se aoueyeg dursoyy 0S’ 900°T “ ~ “t = yt poafaoay Spuapiaicy puu 4 sate]
00'D00'T =~ a A ~ a ~ $aj0N pammoasay) 7O aseyoitig LOFLE ie ba ee ” 4 9961 ‘A[n[ 3ST 2 SoueTeg BuIadQ
: ¢
SLINAWAYd SLdldDa
L961 ‘ANN WO GHANA YVAA AVL HOA SLNAWAVd CNY SLdIGOdH AO INAWALVLS
GNA HOWVaSSY DALLNaIDG UNV LNAWAOCK
CGaLVYOdHOONT VITVHLSNV HLNOS dO ALAIOOS 'TVAOY HHL
REPORT ON ACTIVITIES OF THE COUNCIL, 1966-67
Summary
200
REPORT ON ACTIVITIES OF THE COUNCIL, 1966-67
Accommodation
The past year has seen several significant devclopments in both the accem-
modation and activities of the Society, Of particular importance has been the
move ta the new rooms, The old rooms were severely limited in both meeting
space and library area and during the year several meetings were of necessity
held in the $.A, Museum lecture room, The State Library has the responsibility
to provide accommodation for the Society and fortunately it has been able to
make available two large rooms at the southern end of the State Library building,
This area should provide suitable and comfortable space adequate for the
Society's library arid meetings for at least some years ahead.
Meetings
Eight mectings were held during the year with an average attendance of
42, a considerable increase on that of previous vears, A total of 13 papers were
read and 7 exhibits. presented.
Subcommittees of Council
During the past two years the Council has appointed several subcommittees
to facilitate dealing with an increasing volume af business. The committees are
elected annually, Rules governing their responsibilities and charter have been
drawn up for incorporation in the By-laws.
Research and Endotement Fund
A change in the Rules of the Socicty in 1965 permitted investment of the
Endowment Fund in fixed interest and equity stock, so that both an adequate
income would be available and its. value would not depreciate. Council has
decided that must of the income from the investments should be used for pro-
motion of research, The snm available at present is $500 per year and this is to
be awarded, at discretion of Council, as vrants in support of research expeditions
and field projects undertaken by members of the Society, The first awards will
be made in 1968. The Exceutive Committee reports to Conncil on the fund
and seeks approval for any transactions which nced to be authorised by two-
thirds of the full Council.
Publications
The Society has been handicapped in publishing the ‘lransactions by some
lack of funds. It has been necessary, with the apparently regular annual rise in
printing costs, to limit the volume size te 200 pp. approximately. ‘The Publica-
tion Committee is responsible for decisions on acceptance, rejection or defer-
ment of submitted papers, all of which are first refereed, and for deciding the
size and composition of the volume, Unfortunately not all papers could be
included this year. Attention is drawn to the instructions to authors at the back
of the volume which have been largely re-written. The Committee dealt with
23 submitted papers during the year of which 17 were accepted for publication
in the current volume. Vol. 90 was issued in December, 1966, and it is expected
the present Transactions will also be issued by the end of the year.
201
Library
The Library, through the considerable effort of the Hon. Librarian, has
been re-organized and is now in its new, more spacious quarters. The Council
agreed that it should be confined to scientific periodicals and with this in view.
the small stock of 300 books and a quantity of maps have been offered to and
accepted by the State Library and The Flinders University. Ultimately, all books
and duplicate periodical material will be similarly transferred. The transfer of
the library to the new rooms took place in July under the direction of the Hon.
Librarian and assistants with the help of State Library staff. This very consider-
able undertaking was achieved smoothly and rapidly within two weeks. There
is now room for at least five years’ expansion. The exchange list now numbers
340 Societies and Institutions; 8 new exchanges of journals not held elsewhere
in Adelaide were approved.
Revision of Rules and By-laws
It was decided last year that the Rules and By-laws should he thoroughly
revised, Unfortunately, this has been delayed by the Secretary's illness, but it
is hoped the revised set will be completed and placed before the Society during
the coming year.
Science Centre
The Council, through its representative Dr. H. B. S. Womersley, took part in
discussions with other bodies on the setting up of a Science Centre to serve all
scientific societies in Adelaide. The necessity for such u centre, once rather
acute, has diminished and as far as the Royal Society is concerned, could not
now be strongly supported. The proposal has been shelyed for the present.
Verco Medal
The Council recommended aud the Society subsequently approved the
award of the Verco Medal for 1967 to Professor L, D. Pryor.
Membership
The membership of the Society now stands at 257; 16 new members were
elected during the year and one resigned. Four members of long-standing in
the Society—Mr. A. G. Edquist, Mr. P. Ifould, Mr. F. M. Angel and Dr. P. 8,
Hossteld—died during the year.
OFFICERS FOR 1966-67
Summary
ROYAL SOCIETY OF SOUTH AUSTRALIA
INCORPORATED
OFFICERS FOR 1966-67
Patron:
HIS EXCELLENCY LIEUTENANT-GENERAL SIR EDRIC M. BASTYAN,
K.CM.G., KBE. CB.
President:
H. B. §. WOMERSLEY, D.Sc.
Vice-Presidents:
B. DAILY, Ph.D. K. R. MILES, D.Sc., F.G.S.
Secretary: Treasurer:
M. J. TYLER F. J. MITCHELL
Editor: Assistant Editor:
J. K. TAYLOR, B.A., M.Sc., B.Sc.Agr. I. M. THOMAS, M.Sc., M.1.Biol.
Librarian: Programme Secretary:
N. H. PEDERI Sea Ph.D., DALC., W. kK. HARRIS, B.Sc.
Members of Council:
J. A. PRESCOTT, C.B.E., D.Sce., RK. V. SOUTHCOTT, D.Sc., M.D.
F.B.S., FIAVA., FR.A.CI, B.S., D.T.M. & IT.
J. T. HUTTON, B.Sc., A.S.A.S.M. D. SYMON, M.Sc.
S. A. SHEPHERD, B.A., LL.B. Cc. B. WELLS, M.Sc.Agr.
Auditors:
Messrs. MILNE, STEVENS, SEARCY & CO.
LIST OF NEW MEMBERS
Summary
1966.
1967.
1966,
1966.
1966.
1967,
1967,
1966.
1966.
1967.
1967,
1966.
1966.
1967.
1967.
1966.
1967,
1967.
1967.
1963.
1962,
1962.
1964,
1965.
1963.
ROYAL SOCIETY OF SOUTH AUSTRALIA
LIST OF NEW MEMBERS
AxuouurcH, P. D,, B.Sc., Dept, of Mines, Box 38 Rundle Street P.O,, Adelaide, S.A.
CALE, R. A., B.Sc. (Hons.), Dept. of Mines, Box 38, Rundle Street P.O,, Adelaide,
CaLuow, q Pa B.Se., ¢/o Delhi Australian Petroleurn Ltd,, 32 Grenfell Street, Ade-
aide, S.A.
Cegartegy Sterae Mary, B.A., B.Ed., Cabra Convent, 225 Cross Road, Cumberland
ark, S.A.
Fremine, H. D., B.E., F.S.A.S.M., M.LE., 104 Marion Road, Payneham, S.A.
ReRNEOY, G, RB. B.Su, Ph.D., The Flinders University, Sturt Road, Bedford Park,
Leg, K, E., D.Se,, Division of Soils, C.S,1,R.O., Private Bag No, 1, Glen Osmond, §.A.
Rutnanp, Prof. R. W. R., B.Se., Ph.D., Dept. of Geology, University of Adelaide,
Adelaide, S.A.
Scorr, I. F., B.Sc. (Hons.), Aust. Mineral Development Laboratories, Conyingham
Street, Parkside, S.A,
Smyrn, D, R,, B.Se. (Hons,), Dept, of Genetics, Australian National University,
Canberra, A.C,T.
Szent-Ivany, J. J. H., Ph.D., F.1.C.E,S., 3 Addison Avenue, Athelstone, S.A.
Turner, A. R., B.Sc., Australian Mineral Developinent Laboratories, Conyingham
Street, Parkside, S.A, f
Wace, N. M.,. M.A., Ph.D., Dept. of Geography, University of Adelaide, Adelaide,
Wa po e, }, R, B., Dept, of Genetics, University of Adelaide, Adelaide. S.A.
Wesker, J. Z., Dipl.Biol. (Zagreh), State Herbarium, Botanic Garden, North Terrace,
Adelaide, S.A.
Wersounne, HK. M. E., M.Sc., 15 Canterbury Crescent, Valley View, S.A.
Wuee tre, J. R., B.Sc. (Hons.), State Herbarium, Botanic Carden, North Terrace,
Adelaide. S.A.
Woop, T. G., B.Sc., Ph.D., Diyision of Soils, C.S.1.R.0,, Private Bag No. 1, Glen
Osmond, S.A,
Wagep, R. G., B.Sc. (Hons, ), Dept, of Mincs, Box 38. Rundle Strect P.O., Adclaide,
S.A,
CHANGE OF ADDRESS
Maconocnis, J. R, B.Sc. (Hons.), Herbarium of the Northern Territory, Animal
Industry and Agricultural Branch, Alice Springs, N.T,
BROWN, H Ge B.Sc,, Ph.D., Geology Dept., University of Western Australia, Ned-
ands, W.A.
Datcarno, C. R., M.Se., c/o Anaconda Aust. Inc., 127 Eagle Street, Brisbane,
Queensland.
Freeman, R. N.. B.Sc., Ph.D., P.O. Box 7727, Johannesburg, Rep, of South Africa,
Suaw, ExizAnerH A., Ph.D., Gray Herbarium, Harvard University, 22 Divinity
Avenue, Cambridge, 38 Mass., U.S.A.
Taxeor, Prof. J, L., M.A., Ph.D., Dept. of Geology, Lakehead University, Port Arthur,
Ontario, Canada.
LIST OF LECTURES, EXHIBITS AND
AWARDS OF THE SIR JOSEPH VERCO MEDAL
Summary
204
Sept.
Oct.,
Nov,
April,
May,
June,
July,
Aug.,
LIST
1966
1966
1966
1967
1967
1967
1967
1967
OF LECTURES GIVEN AT MEETINGS DURING
THE YEAR 1966-67
me Ae W. Pargin: “A Local Perspective on Energy from the
arth”,
Dr. Kk. Ler: “Animal Life in the Sail”.
De, KR. F, Ewrr, “The Innate and Learnt in the Behaviour of
Mammals”.
Dr. Dairy delivered his 1966 Presidential Address entitled; “South
Australia in the Cambrian World”.
Dn. P. Mines: “Plant Bugs and Galls”.
Dr. N. M. Wace: “The Southern Continents—Evolutionary Cul-de
sacs or a Fragmented Biotic Realm”.
Pror. R, J. Wrrtrn: “Some Applications of Space Photography”.
Dr. R. Carrick: “The Wildlife of Macquarie Island”.
EXHIBITS
Mr. B. P, THomson: Some Recent Maps Issued by the Geological Survey of S.A.
Dr, J. V. Posstncuam: Effects of Nutrient Deficiencies on Chloroplast Structure.
Dr. R. 'T. Lance and Mr. W. K. Harris: Eocene Leaf Cuticles and Spores and
Pollen from Maslin Bay, S.A,
Mr. H. Mincaam: A Juvenile Echidna.
Mr. CG, Boomsma: Eucalypts from the Victoria Desert.
Mr, I. M, Tuomas: Barnacles from Whales.
Dn, H. M. Laws: The Sea Urchin Centrostephanus, Newly Recorded from S.A.
AWARDS OF THE SIR JOSEPH VERCO MEDAL
1929 Pror. WauteR Howecntn, F.G.S,
19380) Jou~ McC, Brack, A,L,S,
1931 Pror. Sm Dovuctas Mawson, O,B,E., D.Sc... BEL. F.RLS.
1983. Pror. J. Burton Cienann, M.D.
1935 Pror. T. Harvey Jounsron, M.A.. D.Sc.
1938 Pror. J, A. Prescorr, D.Sc,, F,A,C,T,
1943. Henperr Womersury, A.L.8,, FURLE.S,
1944 Pror. J. G. Waop, D.Se., Ph.D.
1945 Crom T. Mapican, M.A., B.E., D.Se., F.G.S.
1946 Hrreert M. TALE, O.B.E
1955 L. Kertu Warn, LS.0., BA. BE. D.Sc,
1956 N. B. TinvAue, ’B.Se.
1957 C, S. Pierre, D.Se.
1959 ©. G. Srerrnens, D.Sc.
1960 Hi. Tl. Finnayson
196], R, L. Specs, Ph.D.
1962 IL G. Axprewarrua, M.Ag.Sc., D.Se,, F.A.A,
19863 N. IT. Limrronx, M.A., Ph is DAC. BAGS.
1965 RK. V, Sovrucorr, D.Sc., M.D,. B.S., D TM, & H.
1966 Pnor. A, R. Atprnman, D.Sc. Ph.D., F.G.S.
1967 L. D. Puyox, M.Se., Dip.For,
For distingnished studies on the genus Eucalyptus, including hybridisation,
controlled pollination and breeding, vegetative propayation and taxnnamy,
and the relation of Kucalypts to mycorrhiza, Other studies have dealt with
poplar growing in Australia.
CONTENTS
S. A. SHepHerp: A revision of the Starfish pests Rips (Astesoiden;
Asteriidae ) aces eh é ‘
J. C. Brmen: Preliminary palaeomagnetic results from the Adelaide System
and Cambrian of South Australia = - - - - - - -
I. A. Mumm™e: On the radioactivity and related fluorescent properties of
sedimentary Australian zircons. - - : 2 = f
I. A. Mumm: Crustal thickness in the South East of seat Australia based
on regional gravity measurements - < 2 z 2
J. E. Jounson and H. eI An aerolite from Soe Sours
Australia - - - - - -
S. J, EpMonps: Paracanthorhynchus galaxiasus, a new genus and species
from a fish, Australian Acanthocephala No. 12 - - = .
J. L. Tazsor: Subdivision and structure of the Precambrian (Willyama
Complex and Adelaide System), Weekeroo, South Australia - -
K, E. Lee: Pheretima tumulifaciens (Oligochaeta, megascolecidae); a new
species of earthworm from the Sepik District, New Guinea = -
N. H. Lupproox: Permian deposits of South Australia and their Fauna -
J. M. Lannsay: Foraminifera and stratigraphy of the Type Ben oe Fort
Willunga Beds, Aldinga Bay, South Australia - = -
Evimaseta A, Suaw: A new species of Eremophila from South Australia
C. M. Purotr and D. R. Smytu: A contribution to our knowledge of
some rare mammals from inland Australia - i: S z x
N. S. Puevce: Fossil Elasmobranch teeth of South Australia and their
stratigraphic distribution eo Se eles e Ser ee ary oe
J. B. Fmmaw: Stratigraphy of late Cainozoic deposits in South Australia
D, E. Pomeroy: The influence of Siemnent on two species of land-
snails in South Australia - - - : : 3 é 3
M. J. Tyter: Microhylid frogs of New Britain - : : 4 i
M. J. Tyter: A new species of frog of , so genus Necsmates from
the highlands of New Guinea - 2
Obituary: Dr. P. S. HossFetp - - - - 7 - s , .
General Account, Library Account - - - - - -« - .
Research Fund - - - - - - : 3 2 é t
Report on Activities of the Council, 1966-67 - : - E " :
Officers for 1966-67 - - - - - - : : : E 2
List of New Members - - - . = ci 5 f 2 E
List of Lectures and Exhibits, 1966-67 - 3 : 2 "
Awards of the Sir Joseph Verco Medal _ - - 2 : = : .
PAGE