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Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 1-6, 1984

ISSN 0035-9173/84/010001 — 06 $4.00/ 1

Chiral Metal Complexes. 15*. Alanine and Proline Complexes of
[N,N -Di(2-picolyl)-LR, 2R-diaminocyclohexane] cobalt (III)

TERENCE J. GOODWIN, ROBERT S. VAGG AND PETER A. WILLIAMS

ABSTRACT.
1k, 2R-diaminocyclohexane,

isolated from the reaction mixture as the least-soluble perchlorate salt.

When Co(II) ions are oxidised in HCl solution in the presence of W,W'-di(2-picolyl)-
R,R-picchxn (L), the diastereoisomer N=B- (Col lol ci0,, ¢Ho0 is

h-@- (Gol Gis] *

reacts with retention of absolute configuration with a variety of ligands including oxalate,

nitrite, S- and R-alaninate and S-prolinate ions.

The products of the reactions have been

isolated and characterised using circular dichroism and high-resolution *H NMR techniques. Both
8, and B5 isomers are formed in the reaction of the parent complex with S-proline and S-alanine.
Only the 8, isomer is formed with R-alanine and no ternary complexes are formed with A-proline.

The reasons for this pattern of reactivity are discussed and means of distinguishing between the

B, and Bo isomers described,

INTRODUCTION

Recently the synthesis and characterisation
of a number of S-alanine complexes of the Co(IIT)
chelate with R- and S-picpnt were reported
(Chambers et af, 1984b; Mulgi et a@, 1984). Only By
isomers were obtained, and it could be shown that
the complexes isolated had resulted from a radical
redistribution of the Co(III) coordination sphere
in that A-8 isomers of S-ala were obtained from
\-a-[Co(R-piepn)Cl2]+ and corresponding A-8 isomers
with one exception, from A-a-[Co(S-picpn)Cla]* .
The other reported reactions of
\-a-[Co(R-piepn) Cla] * have revealed that the
complex can undergo a variety of inversions of
absolute configuration with respect to the metal
centre (Chambers et af, 1983; 1984a). Thus it
emerges that the optically active picpn ligand is
not as highly stereospecific as was first thought
(Cragel and Brubaker, 1972). In order to study
further the chiral discriminations important in
these kinds of complexes we turned our attention
to related species containing 2,Ak-picchxn, which
were expected to be somewhat more stereoselective.
We report below the results of our investigations,
which have included several kinds of monodentate
and bidentate ligands.

EXPERIMENTAL
R,R-Picchxn.4HCl (L. 4AHCL)
This ligand was prepared using a method

modified from that of Hafeli (1975). A solution
of freshly distilled pyridine-2-aldehyde (24.0g,

* Part 14 is Chambers et a@,1984b.

Tt picpn = 2,5-diaza-3-methyl-1 ,6-di(2-pyridyl)hex-
ane, &,R-picchxn = W,N'-di(2-picolyl)-12, 2k-diam-
inocyclohexane, alaH = alanine, proH = proline,
en = 1,2-diaminoethane, trien = 1,4,7,10-tetra-
azadecane, picbn = 2,5-diaza-3,4-dimethyl-1 ,6-
di(2-pyridyl)hexane.

The reactions are compared with similar ones in related systems.

0.224mol ) in DMF (50cm?) was mixed quickly with a
solution of 12,2k-diaminocyclohexane, prepared
using Whitney's (1980) method (12.3g, 0.108mol) in
DMF (50cm3) and then left to stand overnight at

room temperature. The resulting colourless crystals
of the Schiff base were collected at the pump,
washed with DMF (20cem3) and then water (10cm’), then
air-dried { Yield: 27.1g }. The diimine (27.0g)
was dissolved in absolute ethanol (150cm3) and was
transferred to a Paar low-pressure hydrogenation
flask. To the solution was added 5% platinum on
carbon catalyst (0.5g) and the mixture was shaken
under hydrogen (ambient pressure) until uptake of
that gas had ceased (3 days). The catalyst was
filtered off and concentrated HCl (35cm?) was added
to the filtrate. The mixture was evaporated to dry-
ness under reduced pressure to; yield a pale green
solid which was recrystallised from boiling ethanol
( Yicid: Si. lewinel.: Found °C;.248.8370, Gals Nj
eS oe Callen tct or GO. a eN Gin, 3: Ge VOR ce dienes
Noelia. te, bs eG

\-B-|Co(R,R-picchxn)Clp|C10,. 3H20

A method similar to that of Bosnich and Kneen
(1970) was employed. To a mixture of &,R-picchxn.
AHC] (5.20g, 11.8mmol) and LiOH.H20 (1.98g, 47.2
mmol) in water (50cm?) was added CoCl2.6H20 (2.75¢,
11.6mmol). The resulting brown solution was
adjusted to pH 9.0 with aqueous LiOH and oxidised
inva Stream Of air for 3 hr. The pH of this
solution was readjusted to 9.0 as above and the
oxidation continued for 24 hr, after which time
concentrated HCl (1.25em3) and concentrated HC10,
(2.5em3) were added slowly with stirring. The
reaction mixture was reduced slowly in volume on a
steam bath and the oily layer which formed was
continuously dispersed by stirring. A red-violet
precipitate formed slowly. After the mixture had
been reduced to about 20cm? it was cooled to room
temperature, with continuous stirring, and the
crystals were collected at the pump, washed with
water and then a little ethanol, and air-dried.

i Wicldss).joe Aner Pound O,) 20.63" Haas 7s Ny
10.25 HOO, 2.3%. "Cale, for: 60 SHo5N/C130/.5Co:
Cp Ont sees allem os HOO s- qs (oul

A-8-[Co(R,R-picchxn) (NO,,),] C10, . 3H,0

4
Sodium nitrite (0.15g, 2.17mmol ) was added to
a stirred solution of A-8-[Co(&,R-picchxn) Cla] C10).
3Ho0 (0.50g, 0.94 mmol ) in water (30cm?) at 60°C,
and the solution was warmed on a steam bath for
5 minutes to yield a golden yellow solution. This
was cooled to room temperature and the golden
needles which had formed were filtered off, washed
with water and air-dried { Yield: 0.45g, 80% }.
The filtrate was evaporated in a stream of air to
yield a further crop of needles which were isolated
as above { Yield: 0.06g, 11%}. The filtrate had
the same circular dichroism (CD) spectrum as the
isolated crystals, which were shown to contain no
nitrito- species by their infrared spectra, which
also confirmed the identity of the two crops
(Nakamote, 1970). { Anad.: Found C, 35.7; H, 4.53
N, 140435 H20, 10.1%. Gale. for C4 gH39NG07171C1Co :
Creer On MH, 5.03 Neos Us 50,9. 0t4).

\-B-[Co(R,R-picchxn) (ox) ]C10,.2H20

Sodium oxalate (0.13g, 0.97mmol ) was added
to a stirred solution of A-B-|Co(R,R-picchxn)C15|
C10) «2120 in water (30cem3) at 60°C. Once
dissolution of the sodium salt was complete the
reaction mixture was allowed to cool to room
temperature and then reduced in volume in a vacuum
dessicator over silica gel to about 10cm”. The
reddish-orange crystals which had formed were
collected at the pump, washed sparingly with ice-
eold water and air-dried, { Yield: 0.31g, 574}.
A further crop { Yield: 0.08g, 15% } was obtained
in the same way as above after reduction of the
volume of the filtrate remaining to 5em?. The
final filtrate had the same CD spectrum as those
of the two crops of the solid product. { Anaé,:
Hound G5i-42.03 H, 5273 N, 9503 HoO; 5.5%. Cale,
for CogHagN 04 QC1Co: Cs) Alieo Ss} He 4.95 NN; Ons
EDO, wore f°.

N-B,-[Co(R,R-picchxn) (S-ala)](C10,)2.3H20 and
\-B2-[Co(R,R-picchxn) (S-ala)](C10,)2

S-Alanine (0.42g¢, 4.72mmol ) was added to a
stirred solution of \-8-[Co(R,2-picchxn) C12] C10).
3H20 (0.50g , 0.94 mmol ) in water (30em?) at 60°C .
When dissolution was complete 1.0 mol dm-3 aqueous
NaOH (1.0cm?,1.0mmol ) was added slowly. The
orange solution thus formed was cooled to room
temperature, diluted five-fold with water and
applied to a column (35x1.5cm) of CM-Sephadex
C-25 cation exchange resin in the Nat cycle with
deionised water as the supporting solvent. The
column was washed thoroughly with water and then
elution was carried out using O.1mol dm-? aqueous
sodium perchlorate. Two orange bands separated
cleanly, and these were collected in fractions
using an LKB 2070 Ultrorae II fraction collector.
Electronic and CD spectral measurements confirmed
that each band consisted of only one isomer. The
fractions from the first eluted orange band were
combined, concentrated in vacuo at 40°C, and the
solution (20cm3) evaporated slowly over silica gel.
After a week the orange crystals of this B82 perch-
lorate salt which had formed were collected at the
pump, washed with ice-cold water and air-dried.

t Yields 0.12. “Anal.. = PoundiC; 39.2508: Auf awenG
Aleokoes Cale. for C54 H3QN504 QClaCo: Gr 39.35 Hy

4.7, N, 10.9% }. The B,- perchlorate trihydrate

complex was isolated from the second eluted band
in a manner analogous to that above. { Yield:
O.34¢. Anal.: Vound “OC; “3623s ts 5275 WN, 10,0;

TERENCE J. GOODWIN AND OTHERS

H20, Si Ours Callies, kor Co71H36N501 301 oCo: GA B62) 5
He wes: Na tOssetoO sn. Coot ays

N-B,-[Co(R,R-picchxn) (2-ala)] (C10,) >. 3H20

The reaction to form this compound, and its
subsequent isolation, was carried out using
R-alanine in the same quantity and mole ratio as
that employed in the S-alanine reaction described
above. Development of the cation exchange column
gave rise to one main orange band preceeded by an
extremely faint one which contained only a trace of
cobalt complex, insufficient to allow isolation,
but with a positive CD spectrum in the visible
region. Using the same techniques as above, the
main band was shown to contain only one isomer, and
was concentrated to yield the 8, perchlorate tri-
hydrate. { Yield: 0.i2¢. AndZ.’: found Clesece;
Bowe My 10.55 Hol, Ss2n. Cale. for
C51H36N5043CloCo: 6G, 36.25 H, S.237 Ny mlOsabsechioO),

7.8% } . The low hydrogen analysis obtained is
due to the loss of the water of crystallization in
the gas stream prior to combustion. This was
confirmed thermogravimetrically; the calculated H
analysis for the anhydrate is 4.3% .

A-8,-[Co(R,R-picchxn) (S-pro)] (C10,)5.2H20 and
N-Bo- [Co(R, R-picchxn) (S-pro)] (C10,)9.2H20

These compounds were synthesised using the
same weights of \-B-[Co(R,R-picchxn) Cl] C10,.3H0
starting material and mole ratio of amino acid and
base and under the same conditions as those employ-
ed for the synthesis of the alanine complexes. The
two 8; and Bo isomers separated into clean bands
on the column, the 85 diastereoisomer eluting first,
and the perchlorate salts were isolated as describ-
ed above. { For the 8, isomer; Yield: 0.21¢.
Anal.; Found C, 38.4; H, 4.0; N, 100; HO; > re
Cale. for C53H36N 504 901 oCo 2. Ch. BOS

N, 10.0; H20, 5.1% .

For the Bo isomer; Yield: 0.04 9. AnaZy == sound:
Cy 29.23 Hy, 5.23 N, TOSO2s.

Several attempts to isolate isomers containing
R-proline gave reaction mixtures containing various
decomposition products of the starting materials
and which gave only transient trace amounts of
orange coloured species when separation by chromat-
ographic means was attempted.

Microanalyses were carried out by Mrs A. Dams
in the Department of Chemistry, Cardiff, and the
water of hydration analyses were performed using a
Stanton-Redcroft TG750 programmed thermobalance.
Infrared spectra were recorded using a Perkin Elmer
257 grating spectrometer and electronic and CD
spectra measured using a Beckman DK2A ratio record-
ing spectrophotometer and a Jobin Yvon CNRS
Dichrographe III respectively. Proton NMR spectra
were recorded at 360MHz using a Bruker WM 360
spectrometer at 298.2K . These spectra were
recorded in D20 and DMSO-dg using DSS or TMS as
internal standards, or in acetone-dg using its ds

impurity as internal standard (2.17ppm) .
RESULTS AND DISCUSSION

The numbering scheme for the protons is shown
in (I), and is based on that used in previous
crystallographic determinations (Mulqi et aé, 1984).
360MHz 7H NMR data for the complexes are tabulated
in Tables 1 and 2 and electronic and CD spectral

CHIRAL METAL COMPLEXES. 15.

data are presented in Table 3. For reference
purposes the 1H NMR spectra of the aromatic regions
for the various complexes are shown in the Figure.

H(43)
H(42)
H(44)
H(C42)
x H(C41)
H(N3)
H(45)
; nf

Ga)

Hafeli (1975) first reported the synthesis of
A-B-[Co(R, R-picehxn) C1] * and the perchlorate
salt we have prepared gives a CD spectrum in conc-
entrated HCl which is qualitatively similar to his.
All three transitions in the visible region of the
spectrum of this ion in HCl solution have positive
CD absorption and this confirms the absolute confi-
guration of the complex as A. The basis for this
assignment has been discussed previously (Bosnich
and Kneen, 1970), and has been confirmed now by a
number of crystallographic analyses inciuding that
of A-a-[Cr(S-picpn) C12] C10, (Hata et a@, 1981) which
is isomorphous with the Co(III) complex (Yamamoto
and Shimura, 1980), and other analogues of en and
trien with Co(III) (Saito, 1979). It is interest-
ing to note that the CD spectrum of the complex
reported here is nearly enantiomorphous to that of
the perchlorate salt B-[Co(S,S-(+)-picbn)C12]*
which was assigned the A absolute configuration on
the basis of its CD spectrum (Bosnich and Kneen,
1970) . The reason given for the preference of hand
in this latter complex was that interactions between
methyl groups of the central ring with the cds-
terminal chelate arm were minimized. Since the
ligand in our work is of opposite absolute configu-
ration, that the opposite hand of the complex was
obtained suggests that such steric interactions may
also be important in the R2,R-picchxn complex. On
the basis of a number of crystallographic studies
of absolute configurations (Saito, 1979), and with
reference to known CD spectra, all of the other
complexes whose preparations are given here may
also be assigned the A absolute configuration, and
thus A-B-[Co(R,R-picchxn)Cl2]* reacts with retent-
ion of hand in all of the substitution reactions
reported here.

We do however wish to draw attention to the CD
spectra of the two A- complexes of S-ala and S-pro
which have 8, topology. In both cases the dominant
CD band in he visible region of the spectrum is
positive in sign, as expected, but a small negative
absorption is observed at longer wavelengths. A
Similar spectral feature was found for the complex
A-Bo-S,S- Co(trien)(S-pro)]*+, whose absolute
configuration also is known from crystallographic

TABLE 1

360MHz +H NMR DATA’ FOR COMPLEXES IN WHICH
CARBOXYLIC GROUPS SHIELD AROMATIC PROTONS

Complex"

if 2 3 4
H(12) Lelie 7.926 7.869 Gua
H(13) 8.250 8. 366 8.341 8.368
H(14) 7.796 7.881 7.902 7.923
H(15) 8.444 8.278 8.408 8.456
H( 42) e102 ale. 7.801 Te 1SS
H(43) 8.120 8.183 Sys 8.160
H(44) 7.436 TeDOT 7.479 Loe
H(A5) 72358 HEOH Wa Tee 7.198
J42,73 7.60 8.02 8.31 7,66
T7374 804 6.61 Mess 7.63
Ja475 5450 5.48 5.62 6.11
Tyo 43 7593 716 7.81 7.89
S43 4, 7456 7.88 7,00 (Ps
Tyz 45 5-82 5.69 5.80 5.91
H(N2) exchanged 7.536 exchanged exchanged
H(N3) exchanged 6,926 exchanged exchanged
H(C11) 4.408 4.398 Ae 303 As 09
H(C12) 4.623 AeA dd 4.482 out)
(C41) 4.382 ed Aohe3 4.458
H(C42) 4.708 45456 4.602 4.619
Joq7,c72. 715492 -15.80 =16.81 a Ge62
Jo47,042 16.97 S2O815. <=VZeN% elaee5
J077,W2 oe
JC72,W2 ene?
J047,W3 SoEOe
042,W3 Id
CH, 1.277 = 1.1628
aH 3.1908 3.8948 4.4019
SCH 3, 0H 6.80" 7.288
NH De 308 exchanged exchanged
NH’ 4.8773 exchanged exchanged
T at 298.2K; Chemical shifts are +0.002 ppm,

coupling constants +0.02Hz.
Complex 7: A-B-[Co L (ox)]* in D50 3;
ae N-B,-[CoL (R-ala)]* in DMSO-d ;
3: \-B,-[CoL (S-ala)]* in D0 ;
ae A-B,-[CoL (S-pro)]* in D20 .

1

These data refer to the coordinated amino
acidate groups .

4 TERENCE J. GOODWIN AND OTHERS

9 8 7 PPM 9 8 7

Figure. 360MHz 1H NMR spectra of the aromatic regions of the complexes.
7: A-B- [Co(R, R-piechxn) (ox)]* ay \-B, -[Co(R, R-picchxn) (R-ala)]** ;
3% A-B, - [Co(R,R-picchxn) (S-ala)]** 7 63 A-B, - [Co(2,R-picchxn) (S-pro)]** ;
5: \-B- [Co(R,R-picchxn) Cly]* ; 63 A-B- [Co(R,R-picchxn) (NO>) 2] * ;
7: \-Bo-[Co(R,R-picchxn) (S-ala)]** ; 8: \-B5- [Co(R,R-picchxn) (S-pro)]**

Solvents are the same as those given in Tables 2 and 3.

studies (Lin and Douglas, 1968; Freeman et aé, 1970). steric and conformational requirements imposed by
This spectral pattern may occur frequently in Bo the 1,2-diaminocyclohexane fragment of the ligand in
complexes of this type. These results are in cont- conjunction with steric interactions between it and
rast with those found for analogous reactions of the cts picolyl group.

\-a- [Co(R-piepn) Cl] * mentioned above and the high ;
degree of stereoselectivity is most probably due to All of the complexes are indeed of B-topology,

CHIRAL METAL COMPLEXES. 15. 5

TABLE 2

360MHz 'H NMR DATAT FOR COMPLEXES IN WHICH
CARBOXYLIC GROUPS DO NOT SHIELD AROMATIC PROTONS

Complex "
5 6 7 8
H(12) Geos 7.809 7.862 7.810
H(13) 8.371 8.304 8.314 8.288
H(14) 7.945 7.881 7.852 7.873

H(15) 9.530 9.018 9.043 She
H(42) 7,866 7.635 7.686 e732

H(43) 8.161 8.115 8.124 8.123
H(44) T5325 5 pel 7.448
H(45) 7449 eel TA 1.628
J72,73 7.66 7.88 7.46 7.76
J13,74 7.82 ES 7.92 1ob0
J14.75 432 als) Bo 5.80
T4943 Veuls 1682 116 WecT
J 43 44 7.62 pPSoit T49 8.08
Ju 45 5.14 Seu 0 4.92
H(N2) 6.670 6.702 7.509 exchanged
H(N3) 6.971 T2710 7.818 exchanged

H(C11) 4.561 Ae led 4.469 4.478
H(C12) heOIe A fe) Ae DAO 4.695
H( C41) WeoT Le 32 ae], Wee
H(C42) 52370 4451 De lZ? D609
Joq7,C72 -15.53 -16.48 -15.80 -16.40
Jo47,C42 -16.17 -17.20 “17/2 -18.45

Jc77,W2 Dio 6.06 ial

Jc72,W2 9.65 Le 16 6.71

Jc47,W3 <0..02 <0.02 <0.02

042,43 5.20 Sis IS) oO ,

CH 1257

onHt See aCe
JCH3,aH 6.62 |

NH 6.666 exchanged
NH’ 4.6302 exchanged
+

At 298.2K 3; Chemical shifts are +0.002 ppm,
coupling constants are +0.02Hz.

u pe ee A-B8 B-[Co£ C1,]* in acetone-dy 3;
6: N-B-[CoL (NO>)5]* in DMSO-dg ;
7: N-By-[CoL (S-ala)]* in DMSO-dg ;
83 A-Bo- cow ( (S-pro)]* in D290 .
§

These data refer to the coordinated amino
acidate groups .

as is revealed by the *H NMR studies. Reasons for
this have been outlined previously (Chambers et aé@,
1984b) on the basis of symmetry considerations. The
#i(45) resonances occur at higher field than those of
fi{15) due to shielding by a pyridyl ring, as indica-
ted in (I). Reference to the Tables and Figure
confirms this suggestion. The assignments given

were made on the basis of spin-decoupling experiments
and by analogy to related picpn complexes (Chambers
et al, 1984b)

An important result of the 1H NMR studies is
that a convenient way to distinguish 8, and B2
isomers fat the complexes B- Le et
acidate)]"* emer gs. In the complexes |- Bi [CoL(ox) |t
\-81- ne ala) |, A-81-[CoL(S-ala)]*+ and its
S-proline analogue, "the Eee H(15) experiences
some electronic shielding effects from the coordin-
ated oxalate or amino acid carboxylic groups. In
D20 or DMSO-dgé solutions this proton is observed in
the NMR spectra between 8.27 and 8.46ppm. The
position of these resonances in such complexes
appears to have little spread. The range 8.31-8.40
ppm in Do20 and 8.23-8.27 in DMSO-dé solutions was
found for five 81 isomers of [co(R, S-picpn) (S- ala)]*
(Chambers et al, 1984b), four of whose molecular
structures have been established crystallographically
(Mulqi et a@, 1984).

A marked contrast is noted (Table 2) for those
complexes in which such shielding does not take
place. The position of the H(15) resonance is dis-
placed some 0.3 to 1.2ppmdownfield from those of
the oxalate and 8; amino acidate complexes, and thus
the assignment of geometrical isomers is entirely
consistent. Further support for the assignment is
lent by the positions of the C43 resonances in the
alanine diastereoisomers. The ,methyl group in
\-8,-[Co(2,R-picchxn) (S- ala)]** is somewhat shielded
by pyridyl ring of the tetradentate, as revealed by
molecular models, but does not experience the same
interaction in either the B, analogue oz in the By
isomer containing f-alanine.

The question then remains as to the absolute
configuration of W2 in the A-8 complexes. Molecular
models suggest that it has S configuration. Because
of the coordination and conformational requirements
of the 1,2-diaminocyclohexane group the alternative
R- configuration would enforce unacceptable strain
in the coordination sphere. Therefore, all of the
complexes are )\-6-S,S- forms . Furthermore, the
coupling constants between H(N2) and H(C11) or
H(C12), in solutions where the H(N2) proton had not
exchanged with the solvent, are in accord with this
assignment.

No Bo isomers of Co(R-picpn) (ala)** were found
in the reactions of R- or S-alanine with the complex
\-a- [Co(R-picpn)C1,]* (Mulqi et a£,1984). The
isolation in this study of diastercoisoners with
this topology may be due to kinetic factors, in that
the \-8-[Co(R,R-piechxn)X2]"* nucleus is apparently

reluctant to rearrange. The absence of some isomers
however, appears to be due to other steric factors.
Molecular models of appropriate diastereoisomers
indicate that the Bo of these A-alanine and A-proline
complexes have considerable non-bonded interactions
with #(15) and the 8, isomer of R-proline also would
contain unfavourable intramolecular interactions
involving the cyclohexane ring. It thus becomes
obvious why these species were not isolated from the
appropriate reaction mixtures.

TABLE 3

TERENCE J. GOODWIN AND OTHERS

ELECTRONIC AND CD SPECTRAL DATA FOR THE
COMPLEXES AT 298K IN AQUEOUS SOLUTIONS

Complex

A=B-[CoLCia)* *
(5)

\-B-[Co L (NO5) 5] *
(6)

A-B-[Co L (ox)]*

(7)
A-8,-[CoL (R-ala)]**

(2)

A-B,-[Co £ (S-ala)]**

(35

\-8,-[CoL (S-pro)]**
(4)

N-B,-[Co L (S-ala)] oe
Ce)

A-Bo-[Co L (S=pro)]**

(8)

(nm)

534
590
516
403

447
L64
BDA
324

483
856
490
364

480
347
506
Beet
30

480
348
492
20)
306

490
355
477
22
280

472
346
eH
4,83
346

492
358
543
487
SED)
284

ex 1073
(dm? mol 71)

ges}

Bree

79

Ae
(dm2 mot!)

+2958
-7.4
-17.1

-8.3
+34.0
-5.7

-18.0
15953
-10.3
-38.0

Recorded in concentrated HCl solution

The high degree of stereoselectivity found in

these complexes has encouraged us to extend
studies to other related chiral tetradentate

systems and to explore these kinds of species with
a view to using them for stereoselective synthetic
catalysts. We hope to report our results on this

work in the near future.

ACKNOWLEDGEMENTS

The authors thank the S.E.R.C. for financial
support and for a scholarship to T.J.G. R.S.V. and
P.A.W. are grateful to the British Council for the
award of Travelling Fellowships.

REFERENCES

Bosnich, B. and Kneen, W.R., 1970. Inorg. Chem. ,
9 2UGMeaey

Chambers, J.A., Goodwin, T.J., Mulqi, M.W., Williams,
P.A. and Vagg, R.S., 1983. Inorg. Chin. Acta,
75, 241 - 247.

Chambers, J.A., Mulqi, M.W., Williams, P.A. and
Vagg, R.S., 1984a. Inorg. Chin. Acta, 87, 55-60.

Chambers, J.A., Goodwin, T.J., Mulqi, M.W., Vagg,
R.S. and Williams, P.A., 1984b. Inorg. Chin.
Acta (In press).

Cragel, J. and Brubaker, G.R., 1972. Inorg. Chen.,
Lis 303-3110;

Freeman, H.C., Marzilli, L.G. and Maxwell, I.E.,
1970. Inorg. Chem., 9, 2408-2415.

Hafeli, J., 1975. PAD Thesis, Nenchatel University,
Switzerland. (Unpubl.).

Hata, Y., Yamamoto, Y. and Shimura, Y., 1981. Bulé,
Chem. Soc. Japan, 54, 1255-1256,

Lin, C.-Y. and Douglas, B.E., 1968. Inorg. Nucé,
Chem. Lett,, 47 15-20.

Mulqi, M.W., Williams, P.A. Stephens, F.S. and
Vagg, R.S., 1984. Inorg. Chim. Acta (In press).

Nakamoto, K., 1970, INFRARED SPECTRA OF INORGANIC
AND COORDINATION COMPOUNDS, John Wiley, New York.

Saito, Y., 1979. INORGANIC MOLECULAR DISSYMETRY.
Springer-Verlag, Berlin.

Whitney, T.A., 1980. JZ. Org. Chem., 45, 4214-4216.

Yamamoto, Y. and Shimura, Y., 1980. Bull, Chen.
Soc. Japan, 53, 395-401.

T.J.Goodwin and P.A.Williams
Department of Chemistry
University College

P.O. Box 78

Cardiff CF1 1XL

Wales (U.K.)

R.S. Vagg

School of Chemistry
Macquarie University
North Ryde

N.S.W. 2113

(Manuscript received 1.2.1984)

Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 7-14, 1984

ISSN 0035-9173/84/010007 — 08 $4.00/ 1

Stratigraphic Revision of the Early Carboniferous Flagstaff
Formation, Southern New England Belt, N.S.W.

I. D. LINDLEY

ABSTRACT.

Recent stratigraphic studies of the expanded Early Carboniferous marine sequences in

the southern New England Belt, New South Wales, have indicated the need for a revision of the

Flagstaff Sandstone of Roberts (1961).
the Flagstaff Formation.

Because of lithological diversity, the unit is renamed
Within the Salisbury-Brownmore district five new members are defined:

the Allyn River, Underbank Mudstone, Brownmore Sandstone, Bandon Grove Limestone and Lostock

Sandstone Members.

(Allyn River Member), to shallow marine-shelfal deposition (Lostock Sandstone Member).

These are indicative of a transition from deep water turbidite deposition

The five

members are correlated with the upper part of the Woolooma Formation and part of the Isismurra
Formation in the Rouchel district, and the Boolambayte Formation in the Gloucester-Myall Lakes

district.

The uppermost unit, the Lostock Sandstone Member, is disconformably overlain by ash-

flow tuff and conglomeratic lateral equivalents of the Gilmore Volcanic Group, representing a
complete marine regression in the southern New England Belt during the Early Carboniferous.

INTRODUCTION

During the past twenty years the original
.stratigraphic subdivisions used by Roberts (1961)
in the Gresford district (Fig. 1) have been
applied to a large portion ofthe southern New
England Belt. While Roberts's (1961) terminology
continues to be useful, the diversity of litholog-
ies mapped away from the type section of the
Flagstaff Sandstone in the Gresford district
warrants revision, and is the purpose of this
paper.

The Flagstaff Formation, here renamed because
of internal lithological diversity, is one of the
most extensive Early Carboniferous units in the
southern New England Belt, outcropping over an
area of at least 1000 km? (Fig. 2). This paper
concentrates on the definition of units in the
expanded marine sequences present in the Salisbury-
Brownmore district. Revision has been facilitated
by the detailed geological mapping of McDonald
(1972), Gordon (1972), Southgate (1972), Sparke
(1972), O'Neil (1972), Hamilton (1972), Hall
(1972), Parker (1973) and Lindley (1976).

STRATIGRAPHY

The Carboniferous sequence in the Gresford
district has been described by Roberts (1961) and
Hamilton et al (1974). In the vicinity of
Gresford, and essentially restricted to the west
of the Camyr Allyn Fault, Hamilton et al (1974)
defined the Mount Rivers Ignimbrite Member. South-
southeast of Gresford they described an informal
unit, Member A, comprising interbedded sandstone
and mudstone.

In the type section in the Lewinsbrook
Syncline, the Flagstaff Formation consists of a
thick sequence of medium to coarse grained lithic
sandstone with minor grey siltstone (Roberts,
1961). East of the Camyr Allyn Fault, in the
Salisbury-Brownmore district, it is possible to
divide the Flagstaff Formation into five domin-
antly marine members. The lowermost member is
turbiditic and is succeeded by a well-bedded

> v7
Le

NEW SOUTH WALES

Armidale
@

SOUTHERN
NEW ENGLAND

Rouchel-~“seJ}yr

Grestord
Sire

v Newcastle

jaar shred Be Locality map.

lithic sandstone and mudstone sequence which may
contain interbeds of coal and carbonaceous shale.
The boundary between these two mudstone dominated
members in their type section is gradational. The
upper members are dominated by thickly bedded units
of sandstone with several interbedded limestone
horizons.

West of the Camyr Allyn Fault it is impossible
to map the boundary between the lower mudstone
dominated units because of its gradational nature,
and/or lateral facies changes within the units. A
lower turbidite unit is recognisable, and is over-
lain by an upper unit of coarse grained sandstone,
similar to that of the Flagstaff Formation in its
type section.

South of Gresford the Flagstaff Formation is
undifferentiated. There is, however, a lower unit
of interbedded mudstone and sandstone which
Hamilton et al (1974) refer to as Member A, form-
ing the subdued countryside beneath the escarpment
of Mt. Ararat. This informal unit is overlain by
an upper unit of thickly bedded lithic sandstone
and conglomerate, which to the south interfingers
with the Wallaringa Formation.

I. D. LINDLEY

Chichester

WwW

\
\
\

|
lees

S
Vat,

THE EARLY CARBONIFEROUS FLAGSTAFF FORMATION

hester

|‘) |

rat

NE
—N

4
@
57

Se Sony

| oe SS Veco

GEOLOGICAL MAP OF THE

DUNGOG DISTRICT, N.S.W.

Undifferentiated

Verulam Oolite Lens

WALLARINGA FORMATION

FLAGSTAFF FORMATION

Lostock Sandstone Member

Bandon Grove Limestone Member
Mt. Rivers Ignimbrite Member
Brownmore Sandstone Member
Underbank Mudstone Member

Allyn River Member

oO | 2 3 4 +5 6km
SS a
SCALE
LEGEND

aR
~

pee

b %
°

Po 0

0-06

Unconsolidated sand and gravel

Lithic sandstone, si/tstone,
conglomerate, ignimbrite

Red lithic sandstone, conglomerate,
lithic tuff and ignimbrite

Green and grey lithic sandstone,
conglomerate and mudstone

Green and yellow-green sandstone,
mudstone and calcareous sandstone

Grey oolitic limestone
Biogenic limestone

Red- brown vitric ignimbrite

Green-grey lithic sandstone, minor
mudstone, conglomerate , limestone
Grey brown muastone, and fine -
grained lithic sandstone
FRhythmically interbedded sandstone
and mudstone, massive conglomerate

Geological boundary: accurate/approximate
Fault: accurate/approximate

Anticline: accurate/approximate

Syncline: accurate/approximate

Strike and dip of bedding

Measured stratigraphic section with reference number

10 I. D. LINDLEY

_East and southeast of Denes the lower
turbidite unit is overlain by medium grained,

grey-brown lithic sandstone, containing interbeds
of conglomerate in the uppermost units.
Brachiopods from the upper part of the Delepinea
asptnosa Zone are present in the sandstone unit
(952001, Clarence Town 1:25 000 sheet).

Flagstaff Formation
Synonymy: Flagstaff Sandstone, Roberts (1961)

Derivation: Named by Roberts (1961) after a
prominent hill known as 'Flagstaff Hill'; the
hill has since been formally named Lords Pillar
(675236, Allynbrook 1: 25 000 sheet).

Type section: Measured along Brandy Creek
from its confluence with Lewinsbrook Creek
(690172) to a ridge crest at 701208 (Allynbrook
1:25 000 sheet). Measured by J. Roberts and re-
ferred to as Section 73.

Thickness: 1220m.

Lithology: The Flagstaff Formation in its
type section is dominated by thickly bedded,
medium and coarse grained lithic sandstone. The
lower (0-270m) and upper (650-1220m) parts of the
section comprise almost continuous outcrop of green
and brown lithic sandstone, with occasional inter-
beds of siltstone. The interval between 270 and
650m is poorly exposed, and contains thickly bedd-
ed, coarse to medium grained lithic sandstone.
Unexposed parts of the sequence are probably mud-
stone.

An interbedded impure limestone identified
as the Bandon Grove Limestone Member is present
949m above the base of the section.

Remarks: The Flagstaff Formation in its type
section conformably overlies the Bonnington
Siltstone and is apparently conformably overlain
by mudstone of the Chichester Formation (Roberts
et al, 1984).

Age: Brachiopod faunas of the Flagstaff
Formation belong to the Deleptnea asptnosa Zone
(Roberts, 1975; Jones and Roberts, 1976; Roberts
and Engel, 1980). Hamilton et al (1974) and
Roberts (1975) considered that the oldest faunas,
from the core of the Hilldale Anticline at
Greenhills, may be transitional between the
Orthotetes australis and Delepinea asptnosa
Zones. The unit is entirely of late Visean
age.

Allyn River Member

Derivation: The Allyn River (Allynbrook
1:25 000 sheet), where the member is well exposed.

Type section: The type section is measured
along Quart Pot Creek from 696273 to 704278
(Allynbrook 1: 25 000 sheet). Section 85 (Roberts,
1975), Fags 2.

Thickness: 740m.
Lithology: In the type section, the Allyn

River Member consists of thinly interbedded sand-
stone and mudstone. The lower 138m of the

section contains sandstone units whose thickness
ranges from 2cm to over llm (average 117cm), and
mudstone units ranging in thickness from 2cm to
380cm (average 33cm). The sand/mud ratio of this
interval is 2.67. The remainder of the section
is comprised of similar lithologies. The sand-
stone is typically medium to coarse grained and
exhibits sedimentary structures typical of
turbidites, including graded, massive, parallel
and convolute laminated bedding in various com-
binations (typically graded, massive, parallel),
as well as dish structures. Mudstones are grey-
brown and well laminated.

Remarks: Considerable regional variation
is present in the Allyn River Member because of its
mode of deposition. A large proportion of the
member is characterised by interbedded fine and
very fine-grained sandstone typical of classical
distal turbidites of the outer fan facies (Rupke,
1978). Best exposures of these sequences are pres-
ent along most of the Allyn River valley, particu-
larly at 601243 (Allynbrook 1: 25 000 sheet).
Medium-fine to coarse sandstone, and conglomerate,
interpreted as examples of proximal turbidites
characteristic of the middle and upper fan facies
(Rupke, 1978) intercalate with the distal
turbidite sandstone and mudstone sequences.
Coarse upper fan channel conglomerates and levee
deposits are well exposed on the Dungog to
Gloucester Road in the vicinity of 873173, 880170
and 902171 (Dungog 1: 25 000 sheet). In the road-
side exposure at the latter locality the channel
conglomerate discordantly rests on sparsely
fossiliferous mudstone. Pebble sandstones with
injection structures and lithic sandstone with
disturbed bedding and dish structure, interpreted
as part of the middle or upper fan facies, are
common in units of the Allyn River Member at many
localities. Sparse fragments of brachiopod valves
and other fossil debris in tyick massive sandstone
also indicate rapid transport.

East of the Camyr Allyn Fault, the member is
characterised by considerable variations in thick-
ness. Maximum recorded thickness of the Allyn
River Member measured along the Williams River at
Salisbury, is in excess of 1000m. The unit
appears to decrease in thickness away from
Salisbury. In the flat-lying sequences west of
the Camyr Allyn Fault thicknesses of the unit are
unobtainable because the base of the member is not
exposed, and there is difficulty in separating the
uppermost units of the member from those of the
overlying sandstone dominated sequences. Within .
the type section of the Flagstaff Formation, the
lower 270m of lithic sandstone may be laterally
equivalent of the Allyn River Member. These sand-
stones may represent a proximal turbidite deposit.

Age: The type section is unfessiliferous.
The unit directly overlies the Bonnington Siltstone
containing faunas of the Orthotetes australts
Zone and is in turn overlain by the Underbank
Mudstone Member containing the Inflatta elegans
Subzone. The Dunvegan fauna (Roberts, 1961),
which occurs northwest of Gresford in the flat-
lying sequences west of the Camyr Allyn Fault,
is assigned to the Inflatta elegans Zone by
Roberts (1975). The unit is thus entirely late
Visean in age.

THE EARLY CARBONIFEROUS FLAGSTAFF FORMATION 11

Underbank Mudstone Member
Synonymy: Wiragulla Beds (in part),
Roberts (1964).
Derivation: Underbank village (Allynbrook
Is 25 000 Sheet).

Type section: The type section overlies that
of the Allyn River Member, and is measured along
Quart Pot Creek from 704278 to 708281
(Allynbrook 1: 25 000 sheet). Section 85
(Roberts, 1975), Fig. 2.

Thickness: 430m.

Lithology: The unit consists of mudstone and
interbedded fine-grained sandstone. The mudstone
is olive-grey to black and contains abundant well-
preserved faunas at various levels throughout the
type section. The base of the unit is gradational
with the interbedded sandstone and mudstone of the
underlying Allyn River Member.

Remarks: The Underbank Mudstone is restric-
ted in outcrop to east of the Camyr Allyn Fault.
In the vicinity of Salisbury and to the west of the
Salisbury Fault, continental sediments intertongue
with the Underbank Mudstone Member. Sections in
the fault block wedged between the Camyr Allyn
and Salisbury Faults contain up to 11m of coal,
carbonaceous shale and white lithic sandstone.

On the Salisbury to Dungog road, 1.5km south of
Salisbury, interbeds or coal and carbonaceous
shale are present over a stratigraphic interval of
at least 115m. This is the easternmost exposure
of continental sediments which intertongue with
the Underbank Mudstone Member. West of the Camyr
Allyn Fault, interbedded coal-bearing sediments
are present in many exposures immediately over-
lying the Allyn River Member, and mapped as un-
differentiated Flagstaff Formation. Carbonaceous
sediments are present north of Halton on the
Salisbury Gap Road, and at 630248 (Allynbrook

1:25 000 sheet). Carbonaceous sedimenés are also
present in the vicinity of the type section of the
Flagstaff Formation, on Parkes Creek Road at
705153 (Allynbrook 1:25 000 sheet).

The poorly exposed interval between 270 and 650m
in the type section of the Flagstaff Formation is
possibly laterally equivalent to the Underbank
Mudstone Member. Similarly, part of Hamilton et
al's (1974) Member A south of Gresford, which
includes the Torryburn fauna (Inflatta elegans
Subzone fauna, Roberts, 1975), and is here mapped
as undifferentiated Flagstaff Formation, is a
lateral equivalent of the Underbank Mudstone Mem-
ber. Underbank Mudstone equivalents, mapped as
Flagstaff Formation, also outcrop at Wiragulla and
contain faunas assigned to the Inflatia elegans
Subzone (Roberts, 1975).

Age: Prolific brachiopod faunas of the member
are assigned to the Inflatia elegans Subzone of the
Delepinea asptnosa Zone. The member is therefore
late Visean in age.

Brownmore Sandstone Member

Derivation:
1:25 000 sheet).

Brownmore Village (Allynbrook

Type section: The type section of the
Brownmore Sandstone Member is measured from
718251 to 725256 (Allynbrook 1: 25 000 sheet)
along a northeasterly trending ridge 2km southwest
of Brownmore and 1.25km east of Black Camp Creek
(Pao 2)

Thickness: 830m.

Lithology: In the type section, the lower-
most part of the member consists of 210m of re-
sistant massive and parallel bedded lithic sand-
stone with conglomeratic bands. The remainder of
the lower half of the section consists of fine-
grained lithic sandstone, interbedded friable mud-
stone and three shelly limestone lenses. The
upper 250m is a massively bedded medium to coarse
grained sandstone. The entire section is
fossiliferous. At the base of the member there is
a sharp boundary between mudstone of the Underbank
Mudstone Member and lithic sandstone of the
Brownmore Sandstone Member.

Remarks: Thickest development of the Brownmore
Sandstone Member is in the Salisbury-Brownmore
district, where over 900m of sediment are recorded.
The member rapidly decreases in thickness away from
this area, and intertongues with undifferentiated
units of the Flagstaff Formation. Lateral equiva-
lents of the member are possibly represented in the
type section of the Flagstaff Formation by lithic
sandstone in the interval between 650m and the base
of the overlying Bandon Grove Limestone Member at
949m.

Age: Brachiopods from the sandstone are
assigned to the Gigantoproductus tenutrugosus
Subzone of the Delepinea asptnosa Zone indicating
a late Visean age.

Brandon Grove Limestone Member

Derivation:
1:25 000 sheet).

Bandon Grove village (Allynbrook

Type locality: The type locality of the Bandon
Grove Limestone Member is in the vicinity of a small
dam in the headwaters of Quart Pot Creek (671252,
Allynbrook 1:25 000 sheet).

Thickness: 13m.

Lithology: The Bandon Grove Limestone Member
is a biogenic limestone composed of crinoid frag-
ments, minor solitary corals and rare brachiopods.
The limestone is usually pure, occasionally contains
large rounded volcanic pebbles, and at the type
locality contains interbeds of fine-grained
calcareous sandstone. In places it grades into a
cross-bedded calcareous sandstone.

Remarks: Maximum thickness of the member is
15m, recorded in the Salisbury district. The mem-
ber decreases in thickness away from the type
locality, and grades into calcareous sandstone
which is often cross-bedded. The sandstone contains
angular and sub-angular grains of quartz, feldspar
and rock fragments cemented by micrite.

Geographically, the Bandon Grove Limestone Member
is restricted to the eastern side of the Camyr
Allyn Fault. The member is present in the type
section of the Flagstaff Formation and is also

12 :

mappable in tne Wiragulla district, south of
Dungog.

The Mount Rivers Ignimbrite Member in the Gresford
district is considered to be an approximate time
equivalent of the Bandon Grove Limestone Member
because of the mutual exclusiveness of the two
members in terms of their distribution. Strati-
graphically, the members are not recorded together
in the same section, and both occur at similar
stratigraphic levels, several hundred metres above
the Inflatia elegans Subzone.

Age: Brachiopods collected from both above
and below and within the Bandon Grove Limestone
Member belong to the late Visean Gtgantoproductus
tenutrugosus Subzone.

Lostock Sandstone Member
Lostock village (Carrow Brook

Derivation:
1:25 000 sheet).

Type section: The type section of the
Lostock Sandstone Member is measured from 657304
to 664304 (Allynbrook 1:25 000 sheet) along a
ridge immediately north of Bullee Coggee Creek,
4km west of Underbank Section 87 Roberts, 1975),
Big 2:3

Thickness: 475m.

Lithology: The lowermost 30m of the member
consists of coarse grey calcareous sandstone. The
remainder of the lower half of the section is
poorly exposed grey mudstone. The upper 315m
of the Lostock Sandstone Member is represented by
thickly bedded medium and coarse grained green
and yellow-green sandstone.

Remarks: The Bandon Grove Limestone Member
and its calcareous lateral equivalents separates
the Lostock Sandstone Member from the underlying
Brownmore Sandstone Member. Unlike the underlying
sandstone, the Lostock Sandstone Member in most
sections is characterised by a fining upwards
sequence. In the type section the upper boundary
of the member is defined by a disconformable
ash-flow tuff unit. North and east of the type
section the ash-flow tuff is replaced by
conglomerate and conglomeratic sandstone. The
first occurrence of conglomeratic sandstone in
sections 90 and 85 (Roberts, 1975) marks the upper
boundary of the Lostock Sandstone Member and the
Flagstaff Formation.

Mapping of the Verulam Oolite Lens in the upper
part of the member, 1lkm east of Chichester village
(Chichester 1:25 000 sheet), suggests that there
may have been a short hiatus following deposition
of the Lostock Sandstone Member. This resulted

in localised erosion of the lens and uppermost
units of the member.

In the Gresford district, mapping (Hamilton et al,
1974; this work, Figs. 2 and 3) indicates that
the Martins Creek Ignimbrite Member, at the base
of the Gilmore Volcanic Group, overlies either the
Flagstaff Formation or the Wallaringa Formation.
The latter unit intercalates with and overlies the
Flagstaff Formation south of Gresford. The
Martins Creek Ignimbrite Member lies between the

I. D. LINDLEY

Lostock
Sandstone
Member

B.G.

Brownmore
Sandstone Member

Underbank
Mudstone Member

Allyn River Member

Fig. 3. Composite stratigraphic column showing
members of the Flagstaff Formation in the
Dungog district: B.G. - Bandon Grove
Limestone Member; M.R. - Mount Rivers
Ignimbrite Member; F.F. - Flagstaff
Formation (sediments similar to those of
the type section); W.F. - Wallaringa
Formation; M.C. - Martins Creek
Ignimbrite Member (of the Gilmore
Volcanic Group).

Gtgantoproductus tenutrugosus Subzone and the
Rhiptdomella forttmuscula Zone (Roberts and
Engel, 1980), and thus it is considered that the
ash-flow tuff at the top of the type section of
the Lostock Sandstone Member is a correlative of
the Martins Creek Member.

The Lostock Sandstone Member is variable in thick-
ness and a short distance southeast of the type-
section consists of up to 930m of fossiliferous
sandstone interbedded with mudstone. Away from
the type area, the member decreases rapidly in
thickness and intercalates with the uppermost part
of the Flagstaff Formation. Sections north and
east of the type section are characterised by
several limestone horizons, one named the Verulam
Oolite Lens.

Age: Faunas from the member are assigned to
the Gtgantoproductus tenutrugosus Subzone, indica-
ting a late Visean age.

Verulam Oolite Lens

Synonymy: Verulam Oolite Member, Campbell
and McKelvey (1972).

Remarks: The Verulam Oolite Lens is a massive,
grey, cross-bedded oolite. Brachiopods from within
as well as above and below the lens have been assig-
ned to the Gigantoproductus tenutrugosus
Subzone. The unit occurs at a similar stratigraphic

THE EARLY CARBONIFEROUS FLAGSTAFF FORMATION 13

level to the type Verulam Oolite Member mapped by
Campbell and McKelvey (1972) in the Barrington
district, 20km east-northeast of the Salisbury-
Brownmore district. Because of the stratigraphic
position of the unit within the Lostock Sandstone
Member it is regarded as a lens for the purpose of
this revision. The Verulam Oolite Lens is not
recorded in section west of the Salisbury Fault.

REGIONAL CORRELATION

The Flagstaff Formation is characterised by
brachiopod faunas of the Deleptnea aspinosa Zone,
and within the expanded marine sequences of the
Salisbury-Brownmore district, Roberts (1975) has
identified two subzones. The Inflatta elegans
Subzone characterises the Underbank Mudstone Member,
and there is some evidence that it is present in
lateral equivalents of the unfossiliferous Allyn
River Member. The Gigantoproductuse tenutrugosus
Subzone is present in the Brownmore Sandstone,
Bandon Grove Limestone, and Lostock Sandstone
Members. The Inflatta elegans Subzone succeeds
the Orthotetes australts Zone, present in the
Bonnington Siltstone.

Rouchel district: Measured sections of the
Woolooma Formation (Roberts and Oversby, 1974)
contain faunas of the Orthotetes australts Zone
in the lower part and Inflatta elegans Subzone in
the upper part. On biostratigraphic grounds, the
sediments containing the Inflatta elegans Subzone
are considered to be lateral equivalents of the
Underbank Mudstone Member and possibly part of the
Allyn River Member. Similarly, the Orthotetes
australts Zone sequence is laterally equivalent to
the Bonnington Siltstone.

The Isismurra Formation,which intercalates with and
overlies the Woolooma Formation, contains four
informal ash-flow tuff units in its upper part
(Roberts and Oversby, 1974). The uppermost of the
informal units, Cli-d, is correlated with the
Martins Creek Ignimbrite Member by Osborne (1928)
and Roberts and Oversby (1974) on both lithologic-
al and geochronological grounds. Ash-flow tuff
unit Cli-c of the Isismurra Formation has been
mapped south of the Rouchel district towards
Westbrook, where it splits into two units of red
ash-flow tuff separated by coarse lithic sandstone.
East of Westbrook and in the Gresford district,
these two units are mapped as the Mount Rivers
Ignimbrite Member. It would therefore appear that
the Flagstaff Formation is equivalent to the upper
half of the Woolooma Formation and upper (but not
uppermost) part of the Isismurra Formation in the
Rouchel district.

Gloucester-Myall Lakes District: In this
region the Boolambayte Formation is of Visean age
(Crane and Hunt, 1980). The unit is overlain by
the Nerong Volcanics which are considered by
Roberts and Engel (1980) and Roberts (in press) to
be a lateral equivalent of the Gilmore Volcanic
Group. A poorly preserved brachiopod fauna collec-
ted near the base of the Boolambayte Formation in
the underlying Wallanbah Formation may belong to
the Orthotetes australts Zone (Crane and Hunt,
1980), suggesting that a greater part of the
Boolambayte Formation is possibly a correlative of
the Flagstaff Formation.

ACKNOWLEDGEMENTS

The author would like to thank Associate
Professor John Roberts, University of New South
Wales, and Fransisca Kasiki, Rabaul, Papua New
Guinea, for critical review and typing, respec-
tively, during the preparation of this manuscript.
The research was conducted during the tenure of
a Commonwealth Postgraduate Award at the School of
Applied Geology, University of New South Wales.

REFERENCES

Campbell, K.S.W. and McKelvey, B.C., 1972. The
Geology of the Barrington district, N.S.W.
Pactftce Geol., 5, 7-48.

Crane, D. and Hunt, J.W., 1980. The Carboniferous
sequence in the Gloucester-Myall Lake area.

J. Geol. Soc. Aust, 26, 541-52,

Gordon, I., 1973. The Geology of the Chichester-
Eccleston District, N.S.W. B.Sc. (Hons.)
Thests, Untv. N.S.W. (unpubl.).

Hadi, G.Gcg O72.
District, N.S.W.
Untv. N.S.W.

The Geology of the Gresford
B.Se. (Hons.) Thesis,
(Unpubl.).

Hamilton, G., 1972.
Vacy area, N.S.W.
Univ. W.S.W.

TheGeology of the Paterson-
B.Se. (Hons.). Thesis,
(Unpubl.).

Hamilton, G., Hall, G.C. and Roberts, J., 1974.
The Carboniferous non-marine stratigraphy of
the Paterson-Gresford district, New South
Wales. <i. Proc. R. Soc. N.SiW., 107, 76-86.

Jones, P.J. and Roberts, J., 1976. Some aspects
of Carboniferous biostratigraphy in eastern
Australia: a review. BMR J. Aust. Geol.
Geophys., 7., 141-151.

Lindley, I.D., 1976.
Booral district.
N.S.W. (Unpubl.).

The Geology of the Brookfield-
B.Se. (Hons.) Thests, Untv.

McDonald, L., 1972. The Geology of the Brownmore
district, New South Wales. B.Sc. (Hons.)
Thests, Univ. N.S.W. (Unpubl.).

O'Neill, D., 1972. The Geology of the Allynbrook
Area, N.S.W. 8.Se. (Hons.) Thests, Untv.
N.S.W. (Unpubl.).

Osborne, G.D., 1928. The Carboniferous rocks
between Glennies Creek and Muscle Creek,
Hunter River district, New South Wales.
Proe. Linn. Soc. N.S.W., 53, 565-87.

Parker, K.A., 1973. The Geology of the Lostock-
Carabolla District, N.S.W. B.Se. (Hons.)
Thests, Untv. N.S.W. (Unpubl.).

Roberts, J., 1961.
district, N.S.W.
95, 77-91.

The geology of the Gresford
J. Proc. R. Soc. N.S.W.,

Roberts, J., 1964. Lower Carboniferous faunas
from Wiragulla and Dungog, New South Wales.
eA EROCe Hh OC Nite Was 97.9 LOS-2a.

14 I. D. LINDLEY

Roberts, J., 1975. Early Carboniferous brachiopod Rupke, N.A., 1978. Deep Clastic Seas, in
zones of eastern Australia. J. Geol. Soc. Aust., SEDIMENTARY ENVIRONMENTS AND FACIES, pp.
22, 1-32. 372-415. H.G. Reading (Ed.). Blackwell
Scientific Publications, Oxford.
Roberts, J., . Carboniferous palaeogeography
and tectonics of Australia. C.r. 9e Congres Southgate, S., 1972. A Geological Investigation
int. Stratigr. Geol. Carb. (In press). of the Bendolba Area. B.Sc. (Hons.) Thesis,

Univ. W.S.W. (Unpubl.).
Roberts, J. and Engel, B.A., 1980. Carboniferous

palaeogeography of the Yarrol and New England Sparke, G., 1972. The Geology of the Dungog
Orogens, eastern Australia. J. Geol. Soc. Area. B.Sc. (Hons.) Thests, Untv. N.S.W.
Aust., 27,: 167-186. (Unpub1.).

Roberts, J. and Oversby, B.S., 1974. The Lower
Carboniferous geology of the Rouchel district,
New South Wales. Bull. Bur. Miner. Resour.
Geol. Geophys. Aust., 147.

School of Applied Geology,
University of New South Wales,
Kensington, N.S.wW., 2033.

Present Address
Esso Papnua New Guinea Inc.,
P.O. Box 536,

Rabaul, Papua New Guinea

(Manuscript received 27.9.1983 )
(Manuscript received in final form 20.1.1984 )

Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 15-34, 1984

ISSN 0035-9173/84/010015 — 20 $4.00/ 1

Multiple Karstification in the Lachlan Fold Belt in New South Wales:
Reconnaissance Evidence

R. A. L. OSBORNE

ABSTRACT.

The Lower Palaeozoic limestone terrains of the Lachlan Fold Belt in New South Wales have
complex petrography, elusive structure and enigmatic karst landforms.

The geological history of

these terrains suggests that they have been exposed to subaerial conditions and thus karstification

on a number of occasions,
Cretaceous to Recent times.

Palaeokarst deposits exposed in caves,
recent karst processes.
can be recognized.
periods of karstification.

most importantly during Middle Devonian,

Permo-Carboniferous and latest

quarries and at the surface have been truncated by more
In some cases many generations of cave sediments and palaeokarst deposits
This indicates that the limestone terrains have been subjected to multiple
The geomorphology and commonly also petrography of these terrains

results from the imprinting of features developed during each period of karstification.

Multiple karstification offers the possibility that limestone terrains may contain information
about events during poorly understood parts of the geological record.

INTRODUCTION

Upper Ordovician to Lower Devonian limestones,
many of which are massive and recrystallized, occur in
the Lachlan Fold Belt in New South Wales commonly
associated with silicic/intermediate volcanics and
shallow water marine facies. Some karstification has
occurred in all but the most thinly bedded and impure
limestones. Significant karsts with well developed
caves are reported from 39 localities within the Fold
Belt (Matthews, 1979) (Fig. 1). The sequence and
timing of karstification in these terrains is
problematical. Jennings (1982) proposed that the
karsts incorporate relic, buried and exhumed
components indicating a compound history of landform
development.

Limestones may be exposed to subaerial conditions
at an early stage in their diagenesis. Studies of
caves in coral islands (Ollier, 1975) have shown that
significant speleogenesis can occur in poorly cemented
limestones. These syngenetic karst features are the
product of what can be the first of many periods of
subaerial exposure and karstification in the post-
depositional history of limestones. Each period of
karstification will produce or modify landform
features and may deeply penetrate the fabric of the
limestone, producing caves or smaller solution
cavities and depositing sediments within them.

PALAEOKARSTS AND MULTIPLE KARSTIFICATION

Palaeokarsts, produced where karst features have
been protected by burial and revealed by later
exhumation, provide evidence for karstification in the
past. Multiple karstification is indicated by the
presence of palaeokarst features, most often
sediments, in limestone terrains that have been
subjected to geologically more recent periods of
karstification.

Multiple karstification has been recognized in
the Carboniferous limestones of the United Kingdom.
For example Halstead and Nicoll (1971) describe
palaeokarst deposits containing Triassic reptile
fossils in Carboniferous limestones of the Mendip
Hills, Sommerset, England where significant caves and
karst features, believed to have originated in the
early Pleistocene, are also developed. Further
evidence, summarized by Drew (1975), indicates that
"there is considerable evidence that the Mendips were
a true karst area possessing some degree of
subterranean drainage in Triassic times". Ford
(1976), using the Permian and Lower Carboniferous
limestones of the United Kingdom as examples,
recognized that "any limestone of appreciable
geological age may have gone through more than one
cycle of karstification" and that "the possibility
of the control of present-day karst drainage by
fossilized systems should not be overlooked",
Buchbinder et al. (1983) have recognised five
episodes of karstification ranging in age from
Turonian to Neogene in the Cretaceous limestones of
central and northern Israel.

Little study has been made of palaeokarsts in
the Lachlan Fold Belt (or indeed elsewhere in
Australia); however, the literature of the Lachlan
Fold Belt indicates that palaeokarsts of supposedly
Cainozoic age may be fairly common features of its
Lower Palaeozoic limestone terrains. Palaeokarsts
have been reported from Canowindra, Molong and
Wellington Caves by Carne (1919), in the deep leads
of the Gulgong Goldfield by Jones (1940) and in
Steeley’s Quarry at Wombeyan by Hope (1982).
Cainozoic palaeokarst can be inferred from the
report on the Cargo Goldfield of Andrews and
Morrison (1915) and is suggested as a possibility in
the Cliefden Caves area by Webby and Packham (1982).

16

R. A. L. OSBORNE

DUBBO

LACHLAN is

Fig.

1

SYDNEY BASIN JVEW CASTLE

ORANGE aa
BATHURST

SYDNEY

WOLLONGONG
Hy

m KARST LOCALITY

—_—_——

—__ SYDNEY BASIN

100km
ee ee et |

Some significant karsts developed on Lower Palaeozoic limestones of the eastern
Lachlan Fold Belt in New South Wales. A, Abercrombie; B, Bungonias; BD,
Bendithera; BN, Borenore; CF, Cave Flat; CL, Cliefden; CP, Cooleman Plain;
J, Jenolan; KY, Kybean; LB, London Bridge; LC, Colong; M, Michelago; MA,
Marble Arch; MF, Mount Fairy; R, Rosebrook; T, Tuglow; TM, Taemas; W,
Wombeyan; WA, Walli; WE, Wellington WJ; Wee Jasper; WY, Wyanbene; Y,
Yarrangobilly.

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT 7)

Palaeozoic palaeokarst has been reported in New
South Wales by Conaghan (in Crook and Powell 1976)
in reference to a "palaeocave" at the boundary
between the late Lower Devonian Garra Formation and
the Upper Devonian Catombal Group at Mountain View,
near Wellington.

EVIDENCE FOR MULTIPLE KARSTIFICATION IN SOME
LIMESTONES OF THE LACHLAN FOLD BELT IN NEW SOUTH
WALES.

A reconnaissance of seven Lower Palaeozoic
limestone terrains in the Lachlan Fold Belt in New
South Wales has shown them to contain evidence for
multiple periods of karstification. The seven
limestones - the Borenore Limestone (at Borenore
Caves), Bungonia Limestone (at Bungonia Caves), De
Drack Formation (at Mt. Fairy), Garra Formation (at
Wellington Caves), Jenolan Caves Limestone (at
Jenolan Caves), Rosebrook Limestone (at Toll Bar)
and Wombeyan Limestone (at Wombeyan Caves) (Fig. 1)
- all contain massive recrystallized facies
(metamorphosed in the case of the Wombeyan
Limestone) in which significant karstification has
taken place. With the exception of the Garra
Formation in which Osborne (1983) recognized two
periods of phreatic speleogenesis at Wellington
Caves and Conaghan (in Crook and Powell (1976)
recognized the presence of Devonian palaeokarst, the
evidence for multiple periods of karstification
presented below has not yet been the subject of
detailed investigation.

1. Borenore Limestone

The Upper Silurian Borenore Limestone (Carne &
Jones, 1919) is a highly altered, massive, crinoidal
limestone - in places extensively brecciated - that
has been used as a source of marble. At Borenore
Caves, west of Orange, three major karst features -
Arch Cave, Tunnel Cave and Verandah Cave - are
developed in the Borenore Limestone.

Arch and Tunnel Caves were described by Frank
(1972, 1973) who noted (Frank, 1973) that "there is
some evidence for fossil karst that has been exhumed
during the development of the Tunnel Cave". Frank
has recognized here the essential characteristics of
multiple karstification, an ancient karst feature
truncated by the development of a more recent one.

Current investigations by the author have
confirmed Frank’s observations and suggest that the
post-depositional history of the Borenore Limestone
may involve at least four periods of karstification.
The earliest period of karstification (which may be
syngenetic) is indicated by the presence of cement-
filled vugs within the limestone. These (Fig. 2 A)
truncate fossils and may be syngenetic or early
diagenetic in origin. A second period of
karstification is indicated by the presence of
laminated sediment that occurs in vertical zones
within the limestone (Fig. 2 B). These sediments
are unconformable with bedding in the limestone and
appear to have been deposited with a high initial
inclination such as occurs in a nothephreatic cave
environment.

The ferruginized sediments in Tunnel Cave which
have been truncated by the development of the

present cave as described by Frank (1973) represent
a third period of karstification. These sediments
are similar to surficial deposits in the area which
underlie basalts and have been interpreted by
Partridge (1976) as Tertiary in age. A fourth
period of karstification was responsible for the
development of the present caves. In Arch Cave,
there is evidence of a later period of speleogenesis
as speleothems have been dissolved away by an
apparently fairly recent period of phreatic
speleogenesis. How this correlated with the events
in Tunnel Cave is as yet unclear.

The Borenore Limestone is overlain by basalt
flows from Mt. Canobolas which have been dated by
Wellman and McDougall (1974) at 12 Ma. Relationship
between the basalt and Arch Cave suggest that at
least some of the cave development seen today pre-
dates extrusion of the basalt: the southern end of
Arch Cave is terminated by a plug of basalt (Fig. 2
C) which shows an ophitic texture in thin section.

2. Bungonia Limestone

A significant karst with many dolines, caves
and a major limestone gorge is developed at Bungonia
Caves, near Marulan, in the Upper Silurian Bungonia
Limestone (Carne & Jones, 1919).

The limestone forms a plateau into which
Bungonia Creek has cut a gorge 400 m deep (Fig. 3).
Caves developed within the limestone mass of the
plateau have horizontal and vertical elements and
are among the deepest known on the Australian
Mainland, extending to 148 m below the plateau
surface.

The age and developmental history of the
Bungonia karst has been the subject of much study
and speculation. Jennings et al. (1972) and James
et al. (1978) attempted to relate the development of
shafts in the caves and the incision of the gorge to
then current ideas of the timing of uplift of the
eastern highlands. Jennings et al. (1972)
unwillingly inferred that the upper levels of the
caves may extend in age to the early Tertiary with
formation of the shafts and gorge taking place in
the early Miocene, their unwillingness being due to
"the freshness of the cave forms and the absence of
demonstrably ancient fill". James et al. (1978)
faced with further evidence as to the antiquity of
uplift in the Bungonia area were able to cite
geological barriers to cave development to break the
nexus between development of the gorge and the caves
and concluded "that most of the caves could be
considerably younger than the rejuvenation which
formed the gorge".

Notwithstanding the conclusions of James et
al. (1978) there is good evidence to suggest that
cave development at Bungonia has taken place in two
distinct phases and that the older phase,
represented by shallow horizontal cave development
close to the plateau surface, may be of considerable
antiquity.

James et al. (1978) describe a "ferruginous
silecrete" in the B.74 doline (Fig. 3) which is
developed at the contact between argillites and
limestone. Its presence, apparently in situ,
suggests that doline development preceeded

R. A. L. OSBORNE

18

A: Polished block of Borenore Limestone showing cement-filled vugs that truncate

Fig. 2

B: Laminated sediments in "pockets" within the Borenore Limestone that

fossils.

Rule 500 mm long.

are unconformable with bedrock.

Lens cap 55 mm diameter.

C: Basalt plug at termination of Arch Cave.

19

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT

South Marulan

BUNGONIA CREEK

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PERMIAN SEDIMENTS

SILURIAN LIMESTONE

Bungonia

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20 R. A. L. OSBORNE

Fig. 4 A: Sediment in B.50 Cave.
cup 55 mm diameter Bs:
exposed in "Sharon Loves Glyn" Cave.

deposition of now ferruginized horizontally bedded
sandstones on the plateau. Jennings (1982)
describes a remnant of former cave passage, now
filled with sediment, exposed in the wall of B.50
Cave. The filled passage (Fig. 4 A) has been eroded
away by the formation of the present cave void
except for a thin remnant in a blade of rock
protruding into the main room of the cave. The
sediment, consisting of limestone and ferruginized
sandstone cobbles in a sandy matrix, is overlain
disconformably by more recent cave loan.

Recent investigations by the author have
revealed further evidence for ancient karstification
at Bungonia. Inasmall remnant cave, west of the
track from Cardinal View to Cooeeing Point,
(identified by the inscription "Sharon loves Glyn")
ferruginized cave deposits are exposed. These
deposits (Fig. 4 B) appear to have been ferruginized
in situ and with the deposit in the B.74 doline are
indicative of karstification prior to the
ferruginization event.

On the basis of the above evidence it is likely
that the Bungonia Limestone has undergone two
periods of karstification, one producing dolines and
caves in the plateau surface prior to deposition of
the sandstones and the incision of the gorge and
another, related to the incision of the gorge,
during which the deep caves were produced.

Note presence of ferruginised sandstone clasts. Lens
Cave sediment that has been iron-cemented in situ
Pocket knife 100 mm long.

3. De Drack Formation

At Mt. Fairy, near Bungendore, sediment-filled
caves are exposed in the walls of disused dolomite
quarries (Fig. 5 A) which worked the Sandhills Creek
Limestone Member of the Upper Silurian De Drack
Formation (Felton & Huleatt, 1977).

Sediments filling the caves are unconformable
with bedding in the bedrock and have complex
unconformable relationships with each other. An
unfilled cave is also exposed in the quarry face.
Preliminary investigation has indicated the presence
of at least five generations of cave sediment being
from oldest to youngest:

1. an indurated laminated clay with sandy
beds and iron rich horizons, (Fig. 5 D)

2. a polymictic conglomerate

3. an uncemented polymictic gravel

4, a red cave earth, (Fig. 5 C)

5. an uncemented talus, breccia (Fig. 5 B).

Some of the cave sediments have been penetrated
by subsequent periods of speleogenesis. This and
the presence of so many generations of cave sediment

indicates that the dolomite has undergone a number
of distinct periods of karstification.

Fig. 5

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT

SARAH gaesce
SSA

AG &
Sagan SoS
<

<= is Sk
ee was

As: General view of the Mt. Fairy Quarries. Limestone body containing Mt. Fairy
Caves can be seen in the distance. Bs: Angular uncemented talus outcropping at
high level in northern quarry at Mt. Fairy GR 368032 BORO 8827-IV-S, 1:25000.
Photo, D.F. Branagan. Cs: Red cave earth filling cavity between older gravel and
limestone exposed in southern quarry at Mt. Fairy. Photo, D.F. Branagan. Ds:
Disconformable boundary between gravel and older laminated clay exposed in
southern quarry at Mt. Fairy. GR. 368031 BORO 8827-IV-S,1:25000. Photo, D.F.
Branagan.

21

22 R. A. L. OSBORNE

4. Garra Formation

The late Lower Devonian Garra Formation
(Strusz, 1965, Johnson, 1975) crops out in the limbs
of a syncline on the eastern and western flanks of
the Catombal Range in central western New South
Wales. Significant caves are developed in the Garra
Formation at Wellington Caves, 8 km south of the
town of Wellington. The stratigraphy of Cainozoic
sediments filling these caves, as described by
Osborne (1983), indicates that two periods of
sedimentation, separated by a period of surface
erosion and phreatic speleogenesis took place
following the initial development of the caves.

Further evidence for two periods of phreatic
speleogenesis at Wellington Caves is found in
Cathedral Cave where speleothem-like deposits have
been removed by phreatic solution and now forms roof
pendants (Fig. 6 A & B).

The two periods of speleogenesis recognized by
Osborne (1983) together with the "palaeocave" of
Conaghan (in Crook and Powell, 1976 and pers. comm.
1984) indicate that the Garra Formation has been
subjected to three periods of karstification, one
during the Late Devonian and two during the
Cainozoic.

5. Jenolan Caves Limestone

The Upper Silurian Jenolan Caves Limestone
(Chalker, 1971) has developed the best known and
most cavernous karst in New South Wales with 262
caves and related karst features presently
documented (Welch, 1976).

Imperial Cave, a tourist cave developed in the
mass of limestone north of the Grand Arch (Fig. 7),
intersects a number of former vugs now filled with
subaqueously deposited carbonate crystals (Fig. 8 A
& B). These palaeovugs appear to have been part of
an old cave system and McClean (1983) considers that
this system of infilled cavities has controlled the
development of parts of Imperial Cave. The vugs
show no sign of major deformation and must have been
excavated and filled prior to the phreatic
speleogenesis of the present cave.

The evidence from Imperial Cave indicates that
two distinct periods of karstification have acted on
the Jenolan Caves Limestone.

Palaeokarst deposits exposed in Cathederal Cave,
Speleothem-like deposit covered by more recent flowstone.

Wellington Caves. A:
Match box 53 mm long.
B: Speleothem-like deposit now forming part of phreatic roof pendant.

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT

Z Z\\ !
7A
EW re) 50 100m

Approximate boundary of limestone

—_—_— —_-—=__— =

Fig. 7 Tourist caves of the northern limestone, Jenolan Caves, after Trickett (1925).
Shaded part of Imperial Cave is where crystalline palaeokarst deposits are
exposed in the cave walls.

23

24 R. A. L. OSBORNE

6. Rosebrook Limestone

The Silurian Rosebrook Limestone (Carne &
Jones, 1919) has been mined in two quarries at Toll
Bar, 8 km east of Cooma. These quarries expose a
number of cavities filled with cave sediments and
basalt. Basalt 5 km east of Toll Bar has been dated
by Wellman and McDougall (1979) at 38 Ma; however,
its relationship with the flow at Toll Bar is yet to
be established.

The basalt fills a number of vertical cavities
(Fig. 9 A & B) and has the form of pillows (Fig. 9
D), rather than core stones, suggesting that molten
basalt flowed into water-filled caves. Laminated
sands and muds, interbedded with quartz-pebble-
gravels underlie the basalt (Fig. 9 C) and in
places mixing has occurred between the sediments and
the basalt.

As well as the sediments related to the basalt,
red cave earths, which preliminary investigation
suggests are post-basaltic, massive clays and
bedding-plane fills are also found in cavities
exposed in the quarries. Although the relationships
at Toll Bar are as yet unclear they do indicate that
karstification has occurred there prior to the
extrusion of the basalt, and that more recent
karstification has taken place resulting in cavities
that have been filled with red cave earth. It seems
likely that detailed research will show that the
Rosebrook Limestone has been subjected to a number
of distinct periods of karstification.

7. Wombeyan Limestone

The Silurian Wombeyan Caves Limestone (Brunker
& Offenberg, 1970) was metamorphosed by the
emplacement of the Devonian Bindook Porphyry Complex
and the intrusion of related granites. A
significant karst containing 233 caves (Dyson et al.
1982) has developed on the limestone which forms a
topographic basin surrounded by hills cf porphyry.

Jennings et al. (1982) discussed the
development of the caves and suggested that the cave
with the highest elevation in the area, Durrins
Tower Cave, may have formed "well back in the
Tertiary".

Fig Tree Cave (Fig. 10), a large self-guided
tourist cave, through which the often-dry course of
Wombeyan Creek flows has features which suggest that
the Wombeyan Limestone has been subjected to a
number of distinct periods of karstification. A
strongly-iron-cemented quartz-lithic-wacke is
exposed in the bed of Wombeyan Creek within the
cave, downstream of the tourist section. This
deposit has an unconformable boundary with the
Wombeyan Limestone and a disconformable boundary
with overlying cemented coarse gravel fill (Figs. 11
A & B). Its outcrop relationships indicate that it
was deposited within a cave passage, eroded and
covered by the gravel and then eroded again during
the formation of the present cave passage which has
removed much of the coarse gravel. The degree of
cementation of the quartz-lithic-wacke suggests that
it is probably the product of a separate period of
karstification to that which is responsible for the
development of the present caves.

Further evidence for an ancient period of
karstification is found in the eastern non-tourist
section of Fig Tree Cave where a laminated clay-
filled passage (Fig. 11 C) is exposed in the cave
wall. This passage is unrelated to the present
development of the cave which truncates it sharply.

The evidence from Fig Tree Cave suggests that
there has been more than one period of
karstification affecting the Wombeyan Limestone.
Fig Tree Cave and many of the other caves in the
area contain extensive deposits of sediments whose
stratigraphy has not been studied and there are many
breccias in the limestone, some of which could be of
a karst origin.

MULTIPLE KARSTIFICATION AND THE GEOLOGICAL HISTORY
OF THE LACHLAN FOLD BELT IN NEW SOUTH WALES

The geological history of the Lachlan Fold Belt
in New South Wales suggests several periods of time
during which Lower Palaeozoic limestones may have
been exposed to subaerial conditions.

In addition to exposure during subaerial
diagenesis, which may have produced syngenetic
karsts, a number of orogenies and well-recognized
erosional events, during which subaerial exposure
could have taken place, have affected the limestone
terrains of the Lachlan Fold Belt in New South
Wales. The likely post-depositional history of the
limestone terrains discussed above is illustrated in
Fig. 12.

While Benambran, Quidongan and Bowning events
may have resulted in subaerial exposure of the older
limestone in the Fold Belt, the earliest period of
post-diagenetic subaerial exposures for which there
is good evidence took place during the Middle
Devonian Tabberabberan Orogeny following the
cessation of "geosynclinal" sedimentation within the
Fold Belt.

Further exposure would have occurred during
Permo-Carboniferous times when much of the Fold Belt
had high relief and valley glaciation was taking
place, and during Mesozoic to Cainozoic times when
the present period of exposure commenced. Each of
these periods of possible karstification is
discussed below and the limestone terrains where
their effects might be recognized are indicated.

a. Syngenetic karstification

The term syngenetic karst was applied by
Jennings (1968) to karst processes occurring
concurrently with the consolidation of Recent
aeolian calcarenites. In relation to the Lower
Palaeozoic limestones discussed here, syngenetic
karst processes are those associated with the
emergence of relatively unconsolidated carbonates
and their subaerial diagenesis. This is equivalent
to the eogenetic stage of porosity development as
defined by Choquette and Pray (1970).

Subaerial diagenesis is widely recognized as
being a significant factor in the post-depositional
history of limestones (Bathurst, 1975).
Unfortunately little study has been made of the
petrography and diagenesis of Lower Palaeozoic
limestones in New South Wales; however, what is

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT 25

Caves. As

Crystalline palaeokarst deposits exposed in the walls of Imperial Cave, Jenolan

Palaeokarst deposit now forming part of phreatiec rock pillar

indicating relationship between palaeokarst and present caves. Field of view

approx 500 x 750 mm.

structure. Tape 320 mm long.

known does suggest that some were exposed to
Subaerial conditions during their early history.

Wolf (1965) noted solution cavities in Devonian
Algal limestones in central New South Wales while
Semenuik (1971) identified subaerial solution
textures in the Ordovician Bowan Park Group and
related them to a vadose or shallow phreatic
subaerial environment. Neuhaus (1982) has described
internal sediment filled vugs within Silurian
limestones at Gleeson’s near Cliefden Cave which may
also be a result of syngenetic karstification.

Until more study is made of the diagenesis of
Lower Palaeozoic limestones in New South Wales it
will not be possible to assess the significance of
syngenetic karstification.

b. Middle Devonian karstification

The Middle Devonian Tabberabberan Orogeny
brought to a close significant carbonate deposition
in the Lachlan Fold Belt in New South Wales and was
followed by the deposition of quartz-rich
terrestrial and marginal marine basinal sediments
during the Late Devonian and Early Carboniferous.
During the orogeny many of the Lower Palaeozoic
limestones could have been exposed to subaerial
conditions resulting in the development of Middle
Devonian karsts.

B: Palaeokarst cavity exposed in cave wall.

Note vug-like

Middle Devonian karstification is described by
Burns (1964) from Tasmania where the unfolded
Eugenana Beds, a sequence of Devonian cave
sediments, are enclosed within the folded Ordovician
Gordon Limestone. As mentioned previously Conaghan
(in Crook and Powell 1976) recognized Middle
Devonian karstification in the Garra Formation near
Wellington. It is likely that further Middle
Devonian palaeokarsts will be found, as many Lower
Palaeozoic limestones are unconformably overlain by
Upper Devonian sediments (e.g. Bendithera Limestone
and Minuma Beds at Bendithera Caves, Narragal
Limestone and Catombal Group near Molong, Jesse
Limestone and Lambie Group at Limekilns).

The effect of Middle Devonian karstification on
later karst development will depend on the intensity
of later (e.g. Kanimblan) deformation. Where this
has been intense, karst deposits will tend to be
sheared and have the effect of changing the
petrography of the limestones. Alternatively where
little deformation has taken place these old karst
features will be more intact and may act as a
controlling factor over later karstification.

26

Fig. 9

R. A. L. OSBORNE

iy x &
ag Rou
Petes
we ME ASE SY
Sea

Ban

RRS

~ ee |

ae eee
Ne eee vor Pot ier Ck
Lea -
BEGINS

Basalt-limestone relationships in quarries at Toll Bar, east of Cooma. Exposures
in quarry at GR 989916 COOMA 8725-IV-S, 1:25000. A: Basalt filling cavity in
limestone. Photo, D.F. Branagan. B: Basalt filling shaft-like vertical
cavities in limestone. Photo, D.F. Branagan. Cs: Basalt filling cavity,
overlying and partially mixing with quartz-rich gravel. Boundary between gravel
and basalt shown by pick. Photo, D.F. Branagan. D: Detail of basalt showing
pillow-like structure. Coin 24 mm diameter. Photo, D.F. Branagan.

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT ay

c. Permo-Carboniferous karstification

Following the Middle Carboniferous Kanimblan
Orogeny terrestrial erosional conditions were
established over much of the Lachlan Fold Belt in
New South Wales. Relations between rocks of the
Fold Belt and the basal strata of the Sydney Basin
indicate a pre-Permian relief of at least 600 m in
the area that now forms the southwestern edge of the
Sydney Basin (Herbert, 1972), and of at least 900 m
in the Mudgee district (Dulhunty & Packham, 1962).

The deposition of glacial and periglacial
sediments in the Tamworth Trough and at the edges of
the Sydney Basin during the Carboniferous and in
much of the Sydney Basin during the Permian
indicates that valley glaciation was active in the
Lachlan Fold Belt during Permo-Carboniferous times
(Herbert, 1980). It seems likely that erosion
associated with the glaciation was responsible for
the removal of much of the previously widespread
Upper Devonian and other cover from the Lachlan Fold
Belt, exposing its limestones to subaerial
conditions. Many of the limestones in the west and
southwest of the Fold Belt have probably remained
exposed to subaerial conditions since this time (or
perhaps for even longer if the ideas of Opik (1958)
who interpreted the landforms around Canberra as
having Siluro-Devonin origins are correct), their
karst development being a product of this long
exposure. It may then be difficult to identify
karstification of Permo-Carboniferous age in these
areas. While it could be possible to argue that
karstification in these areas has been essentially
continuous since the Palaeozoic, major periods of
folding and uplift would ensure that karstification
was episodic.

Some limestones to the east of the Fold Belt
were exposed in an environment of high relief during
Permo-Carboniferous times and then covered by
sediments of the Sydney Basin which protected them
from further karst action until at least the Late
Cretaceous. In these limestones (e.g. possibly the
Jenolan Caves Limestone, Bungonia Limestone and the
limestones at Billy’s Creek, Brogan’s Creek, Colong,
Church Creek and Portland) it may be possible to
identify Permo-Carboniferous karstification.

The proximity of the plateau surface at
Bungonia Caves to the level of the basal
unconformity of the Sydney Bain exposed in the
Shoalhaven Gorge suggests that the plateau surface
may be an exhumed Permian landscape (Young, 1977).
Wass and Gould (1969) identified Permian sediments
overlying the Bungonia Limestone in the South
Marulan area, north of Bungonia Gorge. These
sediments have a basal elevation of approximately
590 m while the plateau in the caves area has an
elevation of about 550 m. Flat lying, often
ferruginized quartzarenites overly the Bungonia
Limestone in the caves area. These were considered
by James et al., (1978) to be Tertiary. However,
Carr et al., (1980) suggest that some may be Permian
in age by analogy with the sediments described by
Wass and Gould (1969). If this is the case then
karst features developed during the Permo-
Carboniferous could have been preserved by the
mantle of the Sydney Basin and then exposed later by
erosion and Cainozoic karstification. This view is
supported by geological reports on the quarries at
South Marulan (Anon, 1972) which state, when

discussing the likely effects of cavitation in the
limestone on quarrying operations, that "At Marulan
much of the cavitation is Permian or pre-Permian in
age" and report a cavity in the quarry containing
lithified fill which has been intruded by dolerite
dykes. As a result of this occurrence Anon (1972)
concludes that "The lithified nature of some of the
infilling and the fact that it pre-dates the
dolerite dykes suggests that it is probably pre-
Permian in age". These dykes are likely to be
related to basalt flows in the Bungonia area dated
by Wellman and McDougall (1974) as Eocene. If this
is the case then the cavitation exposed in the
quarries is probably Permian in age. The sediments
in B.50 Cave, described by Jennings (1982) (see
above), have the type of relationships one might
expect from Permian cave deposits. However, they
contain clasts of ferruginized sandstone and are
therefore more likely to be early Tertiary in age.

Jenolan Caves is another area that would have
been close to the surface (and possibly exposed)
during Permo-Carboniferous times and then covered by
the edge of the Sydney Basin. The elevations of the
Sydney Basin outliers near Jenolan Caves suggest
that the area had a high relief during Permo-
Carboniferous times making the Permian surface more
difficult to define than in the case of Bungonia.
The crystal sediments in Imperial Cave (see above)
have the relationship with the present caves that
one might expect from a Permian palaeokarst deposit.

dad. Cainozoic karstification

During the Cainozoic the Lower Palaeozoic
limestone terrains of the Lachlan Fold Belt in New
South Wales have been subjected to significant
subaerial exposure. This has been punctuated at
some localities by the extrusion of Tertiary basalts
and by the deposition of thin (?) Tertiary cover
which has in places been lateritised. The
occurrence of karstification during the Cainozoic
has never been in dispute but its timing presents
considerable problems.

With the exception of palaeokarsts it has been
traditionally accepted that karsts, like other
landforms, are a product of events taking place in
the most recent part of the geological timescale.
This view has been applied by many workers to the
Lower Palaeozoic limestone terrains of New South
Wales.

Sussmilch and Stone (1915) when discussing the
likely age of Jenolan Caves state "it is therefore
quite improbable that the age, even of the oldest of
the caves can exceed 500,000 years". A similar
timescale for Cainozoic karstification has been
accepted by many recent workers. Frank & Jennings
(1978) have epiphreatic action ceasing in the main
Arch at Abercrombie Caves by 15 Ka while Jennings et
al. (1972) and James et al. (1978) cite evidence
that suggests an old age for karstification at
Bungonia Caves but recoil from its implications.
Notable exceptions to the idea of young karsts have
been Francis (1973) who suggested that phreatic
speleogenesis at Wellington Caves may have taken
place during the Miocene and Connoly and Francis
(1979) who suggested a Cretaceous age for Main Cave
at Isaacs Creek (at Timor in New England Fold Belt).

28

Fig.

R. A. L. OSBORNE

za

KOORINGA

Collapse Doline

Fig Tree Entrance

100m

10 Fig Tree - Creek Cave System, Wombeyan Caves, after Trickett (1899).
Location of quartz-lithic-wacke outcrop. Bs: Location of clay-filled passage.

As

Fig.

11

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT

As Quartz-lithic-wacke exposed at locality A Fig. 10. Note steep nature of
boundary between wacke and limestone (just right of lens cap) and development of
scallops on both wacke and limestone. Lens cap 55 mm diameter. Bs
Disconformable boundary between quartz-lithic-wacke (right) and coarse cemented
gravel (left). Note erosional nature of boundary near point of pencil. C:
Clay-filled passage exposed in wall of Fig Tree Cave at locality B Fig. 10. End
of tape points to outline of passage.

29

R. A. L. OSBORNE

30

suefequiom ‘mM fueg
TIOL ‘qL ‘uetouer ‘rr ‘fuoqZuTTIem ‘GM SAuTeg *qW SAW ‘feTuoZung ‘gq feucuaeu0g
‘Nd cdoded styq uy pessnosTp SuTe4ueq SUOJSOMTT soy queyd queag - OTL 21 °8Ty

NVIYNTIS

OSNINMOG
NVdsasevesgEevl

NVINOAJG

HE

NV TEWINV

oie al

NVINYSd

NOILISOd3G ANOLSAWNIT aes

AN35O8O WKY

WSINVOINA
ALVIGAWYSLNI/OIONMNS

JISSVIGL

a . oa)
: g g a cm
2
é
«

oissvanr

NOISNYLNI

NOILVLNAWIGAS ANIYVAN

NOILVLNAWIGSS ANIYVN-NON

Y3AO9 Livsva |:
aasodXann WW
dasodxa a

JNIZOOIN

3N390I1d |

MULTIPLE KARSTIFICATION IN THE LACHLAN FOLD BELT 31

Fig.

m. Photo, T. Allan.
development.

Recent work on the history of the Great Divide
and on the age of landforms in southeastern
Australia based on the radiometric ages of basalts
has brought into question the long accepted concept
of a Late Pliocene uplift followed by a period of
rapid erosion. Significant work by Wellman (1979),
Jones & Veevers (1982) and Bishop (1982) suggests
that uplift of the Southeastern Highlands began
between 50 - 90 Ma ago and that minimal erosion or
change in drainage direction has occurred in the
past 40 Ma. Similar reasoning has led Young (1983)
to suggest that the rates of denudation in
southeastern Australia are much lower than those
usually accepted.

If these newer ideas are correct then either
the caves and karsts are young features of old
landscapes as inferred by James et al. (1978) or
there is need for a complete revision of currently
accepted views on the timing of Cainozoic
karstification. Osborne (1983) has shown that
speleogenesis at Wellington Caves involved two
distinct phases during the Cainozoic while the
features described at Borenore, Bungonia, Mt. Fairy
and Toll Bar are indicative of multiple periods of
karstification during the Cainozoic. It seems
likely that further examination will show this to be
the norm.

13 Palaeokarst deposits exposed in Main Cave (TR.1) Isaacs Creek Caves. A:
deposits truncated by present cave development.

Field of view approx. 2 m x 2.4 m.

? Pool
Field of view approx 1.6 x 1.4
B. Flowstone completely truncated by phreatic

Photo, T. Allan.

The relationship between karst features and
basalt at Toll Bar and Borenore indicate that
significant karstification took place earlier in the
Cainozoic than had been usually inferred. Recent
work by Goede & Harmon (1983) has shown that some
stalagmites deposited on gravelly alluvium in pais
Cave, Tasmania are beyond the range of 2309n/23 U
dating (over 400 Ka) also indicating that extant
caves may be older than has been previously thought.

If the Lower Palaeozoic limestone terrains of
New South Wales have been subject to multiple
periods of karstification within the limits of the
Cainozoic and karstification has taken place earlier
than the Late Pliocene then existing models for
landscape evolution and speleogenesis, based on the
concept of a single latest Cainozoic cycle of
development, cannot be maintained.

MULTIPLE KARSTIFICATION OUTSIDE THE LACHLAN FOLD
BELT

Multiple karstification can occur in any
limestone of geologically significant age and is
likely to be widepread in the Palaeozoic limestone
terrains of Australia. At Torrawangee Quarry, 70 km
north of Broken Hill, Branagan (1984) has postulated

32 R. A. L. OSBORNE

Palaeozoic cave sediments occur within the Late
Proterozoic limestone of the Wammerra Formation
(Cooper & Tuckwell, 1978); much younger cave
sediments also occur here within this Formation.
Reconnaissance of caves at Isaacs Creek (Fig. 13) in
Middle Devonian limestone of the Tamworth Trough
(New England Fold Belt) has indicated that multiple
karstification has occurred there also.

CONCLUSIONS

The Lower Palaeozoic limestone terrains of the
Lachlan Fold Belt in New South Wales have been
subjected to multiple periods of karstification.
There is good reason to believe that at least some
of the limestone terrains were exposed to subaerial
conditions and thus karstification during Middle
Devonian and Permo-Carboniferous times and that some
karst elements produced during these times may
survive today.

At least one limestone, the Garra Formation at
Wellington Caves, has undergone more than one cycle
of karstification during the Cainozoic and it seems
likely that this has been the case elsewhere.
Relationships between karst landforms and Tertiary
basalts and sediment, particularly at Toll Bar,
indicate that karstification has occurred much
earlier in the Cainozoic than has been generally
accepted. This brings the age of karst landforms
into line with recent concepts as to the antiquity
of uplift and landforms in the Southeastern
Highlands of Australia.

The recognition of multiple karstification
allows Lower Palaeozoic limestone terrains to be
interpreted in a new way. Firstly it introduces a
new factor into their post-depositional history,
that of multiple subaerial exposure, which may help
to explain some of the complexity of their
petrography and geomorphology and, secondly, it
raises the possibility that evidence may exist, in
the form of palaeokarst deposits, of what
terrestrial conditions were like during the
Tabberabberan Orogeny, the Permo-Carboniferous and
during poorly-known parts of the Cainozoic.

ACKNOWLEDGMENTS

This paper is a result of the author’s
continuing postgraduate studies in the Department of
Geology and Geophysics, University of Sydney.
Associate Professor D.F. Branagan who is supervising
the research has provided much in the way of
encouragement, enthusiasm and criticism.

Access to Jenolan and Wombeyan Caves has been
granted by the Director, Department of Leisure,
Sport and Tourism and to Wellington Caves by
Wellington Shire Council. The staff of both these
organizations have been most helpful.

Associate Professor Branagan, A. Allan and T.
Allan have assisted with the field work. G. Francis
and J.M. James assisted by reading the manuscript,
C.A. Johnson with proof reading and D. Garbler with
typing the drafts.

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STRUSZ, D.K., 1965 - A note on the stratigraphy of
the Devonian Garra Beds of New South
Wales. J. Proc. Roy. Soc. N.S.W.98 : 85-
90.

SUSSMILCH, C.A. and STONE, W.G., 1915 - Geology of
the Jenolan Caves District. J.Proc. Roy.
Soc. NeS.We 49(3) : 332-384.

TRICKETT, 0., 1899 - Progress and other reports on
the limestone caves for the year 1899.
Ann. Rept. Dept. Mines N.S.W. 1899 : 210-
213.

TRICKETT, 0., 1925 - The Jenolan Caves, New South
Wales (map).

Department of Geology and Geophysics,
University of Sydney,
N.S.W., 2006, Australia.

WASS, R.-E. and GOULD, I.G., 1969 - Permian faunas
and sediments from the South Marulan
district, New South Wales. Proc. Lin.
Soc. N.S.W., 93 : 212-226.

WEBBY, B.D. and PACKHAM, G.H., 1982 - stratigraphy
and regional setting of the Cliefden Caves
Limestone Group (Late Ordovician), central
western New South Wales. J.geol. Soc.
Aust. 29 : 297-317.

WELCH, B.R., ed. 1976 - The Caves of Jenolan 2: The

northern limestone. Sydney University
Speleological Society, Sydney, 131 pp.

WELLMAN, P., 1979 = On the Cainozoic uplift of
southeastern Australian highland. J.
geol. Soc. Aust. 26 : 1-9.

WELLMAN, P. & McCDOUGALL, I., 1974 - Potassium-argon
ages on the Cainozoic volcanic rocks of
New South Wales. J. geol. Soc. Aust.
21(3) : 247-272.

WOLF, K.H., 1965 - Petrogenesis and palaeoenviron-
ment of Devonian algal limestones of New
South Wales. Sedimentology 4: 113-178.

YOUNG, R.W.,
Shoalhaven catchment.

1977 - Landscape development in the
Z. Geomorph NE. 21

YOUNG, R.W., 1983 - The tempo of geomorphological
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Australia. J. Geol. 91 : 221-230.

(Manuscript received 2.2.1984)
(Manuscript received in final form 19.4.1984)

Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 35-44, 1984

ISSN 0035-9173/84/010035 — 10 $4.00/ |

The Stratigraphic Palynology of the Murray Basin in
New South Wales. II. The Murrumbidgee Area

HELENE A. MARTIN

ABSTRACT. This report on the stratigraphic palynology of the Murrumbidgee area on the eastern
edge of the Murray Basin agrees in a general way with an earlier one (Martin, 1977). However,
many more bores have been examined since the first report, including a number of deep bores
which extend to basement, so that more precision and detail is presented here.

The basement assemblages 4T©€ Early and Late Permian and Early Cretaceous.

The oldest Tertiary assemblages are the Mid-Late Eocene Middle Nothofagidites asperus Zone.
The latest Eocene-earliest Oligocene Upper N. asperus Zone reported in Martin (1977) has not
been found in any other bore. The thick sections of the Oligocene through Early Miocene
Proteacidites tuberculatus Zone with almost uniform assemblages have been subdivided using

quantitative events of three selected taxa.

There are a few occurrences of the Mid-Late

Miocene Triporopollenites bellus Zone, after which pollen is usually not recovered. There are

two records of Pliocene assemblages.

Some dinoflagellates are found in bores near Hay.

They indicate channels or low-lying depress-

ions which became flooded by the Early-Mid Miocene high sea levels, rather than truly marine

conditions.

The quantitative events (i.e. the high ratios) used here to subdivide the P. tuberculatus Zone

show a reasonable correspondence to changing sea levels.

The species of the more swampy hab-

itats are more abundant at the time of high sea levels whereas the species requiring well
drained habitats become more frequent at times of low sea level.

INTRODUCTION

Martin (1977) has described the stratigraphic
palynology of the Murray Basin in the Hay-Balran-
ald-Wakool Districts. This report included two
deep bores which extended to the Mid-Late Eocene
Lower Nothofagidites asperus Zone. Most of the
bores however were discontinued before reaching
the depths of this zone. This study reveals
thick sections of the Oligocene through early
Miocene Proteacidites tuberculatus Zone.

Many bores have been examined since this
report, including a number of deep bores which
extend to basement below the Tertiary. The thick
sections of the P. tuberculatus Zone, with no
reliable means of subdividing it, have been a
problem. The Water Resources Commission of New
South Wales requires some stratigraphic control
within this zone for groundwater exploration.
For this purpose, certain quantitative features
have been investigated and found suitable for
stratigraphy. This paper presents the stratigr-
aphic palynology of ihe Tertiary and basement of
the Murray Basin in the Hay, Deniliquin and
Narrandera districts. None of the results in
Martin (1977) have been changed; indeed they
have been confirmed with more detail and precis-
ion in this report.

GEOLOGY

The Murray Basin is essentially a Cainozoic
feature but it overlies infra basins of Palaezoic
and Mesozoic age (Bembrick, 1975). Pollen assem-
blages of Early Cretaceous, Early and Late

Permian have been recovered from basement assemb-
lages. The sediments of these ages are hardly any
different to those of the Cainozoic and it may be
impossible to distinguish between them without a
palynological examination.

The Tertiary marine transgression extended as
far east as Balranald, and its probable limits are
shown on Fig. 1. Dinoflagellates which indicate
marine or brackish water conditions have been
found in significant numbers in two bores at Hay
and very minor occurrences in several other bores
elsewhere. Otherwise, the whole of the area is
completely non-marine.

A number of stratigraphic units have been des-
cribed by different authors for different parts of
the Basin. For the region under study here,
Woolley and Williams (1978) and Woolley (1978)
have adopted the units used by Lawrence (1975) for
the Victorian part of the basin, with slight
modification. The unit formerly known as the
Renmark Beds (used in Martin, 1977) has been sub-
divided into the Warina Sands and Olney Formation.
The basal unit encountered in this study is the
Mid-Late Eocene Warina Sands which was deposited
under generally non-marine conditions. It cons-
ists of coarse-grained quartz sands with minor
dark grey clay lenses and carbonaceous layers. It
is found only in the deeper parts of the basin and
does not extend east of Hay. The overlying unit,
the Olney Formation, was deposited under deltaic,
fluvial and lacustrine environments. It is dom-
inated by thick lignite layers and contains grey

36

carbonaceous clay and extensive sand lenses. The
basal part of the Olney Formation is Eocene, and
in this non-marine region, extends probably to
the Miocene.

The Wunghnu Group (used in Martin, 1977)
which overlies the Renmark Beds in the non-marine
eastern part of the Basin has been subdivided in-
to three units. One of these, the Torrumbarry
Clay, does not form a definite, mappable unit in
this area (Woolley and Williams, 1978), so is
not discussed further. The Calivil Sand overlies
the Olney Formation. This unit is dominated by
coarse sand and fine gravel, usually pale grey to
white, or pale brown. It also contains very
minor bands of carbonaceous clay. The unit be-
comes more clayey towards the west and is thought
cCoabe Late Miocene. to Plaocene inc age. The
Shepparton Formation, the uppermost unit, over-
lies the Caliavil Sand. It is characterised. by
polymict sand with yellow and brown the dominant
colour, and variegated (white, yellow, red-brown,
prey) clay. It 1s thought to be Late Pliocene
and Pleistocene in age.

The boundaries between the three units which
occur over most of the area are not always clear
because of the similarities of the lithologies.
The definition of the top and the base of the
unit is often rather subjective (Woolley and
Williams, 1978). The sequence of carbonaceous,
mostly pale grey, then variegated sands and clays,
which fits the Olney, Calivil and Shepparton units
respectively, 1S clearly seen in all of the bore
logs. Some of the logs have these units marked
on them, but when they are compared with the

HELENE A.

MARTIN

boundaries, no attempt is made to fit the palynol-
Ogy.into these units. In any case, the ages
assigned to these formations by Woolley (1978) and
Woolley and Williams (1978) are based mainly on
palynology of Martin (1977, unpubl. and pers. comm).

Framework tectonics are regarded as the primary
control of the Murray Basin (Brown, 1983). The
basement features of Paleozoic or Mesozoic age are
Still active and there have been movements along
the faults.in Tertiary time: The basement highs
and lows have retained their relative positions
throughout Tertiary time (R.M. Williams, pers.
comm.). The basement over most of the Murrumbidg-
ee area is relatively deep, and under tthese
circumstances, the sediments are reasonably well
preserved. Sediment accumulation has been sensit-
ive to eustatic changes which, however, is regard-
ed, as a secondary influence (Brown, 1983). Changes

in sea level have the greatest influence on depos-

ition close to the sea, but with increasing dis-
tance from the sea, the influence decreases. In
this non-marine area, the Late Miocene depositional
hiatus (in Brown, 1983) is recognised, but the
Mid-Oligocene hiatus cannot be identified (R.M.
Williams, pers. comm.).

Only the consistently grey clays yield pollen.
Once brown, yellow or red colours appear in the
section, even in quite minor quantities, the
samples are usually barren. The very pale grey
clays are frequently barren also. Sands do not
yield pollen but very minor clay lenses or sand
with a substantial silt and clay matrix may be
suitable for palynology. Consequently units mapp-
ed as sand may have yielded pollen assemblages.

palynology, the boundaries do not always coincide
and there is variation from one bore to another.
Because of these difficulties in defining the

a >

<
026201 Cl 36267

7 360256 es os
30464
Jo tras an 30422 <
“bee pf 0443\ |3se366 Xt
/ ver Hay saan 036368
pipes 36229 eae eease \ Narrandera
/ 30435¢e 3088 Alias). ¢
30362 36373 | a
\ ©36235 A
| 36211 36040 >
30959° 30320
| 036240 30323 Probable extent of
©36069 A —— marine Tertiary
e
rf Bezecr ge3e° Ce30497 i, A — A Margin of Basin
“re, 36102 PJerilderie W ° Bore
a a Veniliquin Ix7. \ A Early Cretaceous
36201 B! v é Late Permian
<e> Early Permian
<e36283 / A—A' Section
a 0 20 40 601m
| fee

Rigid

Locality Map.
from Bembrick (1975).

The probable extent of the marine Tertiary and the margin of the Basin are

PALYNOLOGY OF THE MURRUMBIDGEE AREA 37

MATERIALS AND METHODS

Samples from some thirty three bores are inc-
luded in this study. Almost all of the samples
are cuttings. Some of the bores have been sunk
with the percussion drill which has a limited
depth. Bores deeper than 120m are usually sunk
with the rotary drill.

The possibility of contamination is greater
with cuttings than with cores and the main sources
of contamination are discussed in detail in Martin
(in press a). However, with care and appropriate
procedures (see Martin, in press a) relatively
clean cuttings may be obtained. Consistent patt-
erns repeatable in bore after bore and barren
samples anywhere in the sequence would not be
possible with appreciable contamination. Occas-
ionally, contaminated samples are detected and
they are rejected. Cuttings supplied by the Water
Resources Commission of New South Wales are suit-
able for stratigraphic palynology and give a body
of internally consistent data.

The samples have been treated with cold hyd-
rochloric and hydrofluoric acids, weak nitric acid
and potassium carbonate solutions. Strew samples
have been mounted in glycerine jelly.

PALYNOSTRATIGRAPHY

1. Permian

Permian palynostratigraphy follows the scheme
set out by Kemp et al (1977). The author citat-
ions of species names may be found in this refer-
ence.

Early Permian assemblages have abundant mono-
saccate pollen and bisaccates are rare. A number
of spores which range through the Early Permian,
e.g. Apiculatisporites cornutus, Microbaculispora
tentula, Cyadopites cymbatus and Horriditriletes
ramosus are found in these assemblages.

PALYNOLOGICAL ZONES
STOVER & PARTRIDGE 1973
PARTRIDGE 1976

Middle ©. bellus
MIOCENE —-— Zone |

Verrucosisporites psuedoreticulatus and Marsupip-
ollenites triradiatus, which first appear at the
base of stage 3a are found in bores 36211 and 36275.
Granulatisporites trisinus, which first appears at
the base of stage 3b, is not found in these two
bores, but it is present in bore 36229, in addition
to the former two. Consequently, the assemblages
in the first two bores are stage 3a and the latter,
stage 3b. In addition to most of the spores already
mentioned, bore 36283 contains Praecolpites sinuosus
which first appears at the base of upper stage 4a.
Spores diagnostic of the overlying upper stage 4b
are not present. Hence this assemblage is upper
stage 4a.

In the Late Permian assemblages, bisaccates
are dominant with very few monosaccates, and there
is a diversity of spores. Didecitriletes ericanus,
which first appears at the base of lower stage 5b
is present in both bores. Dulhuntyispora parvith-
ola, which first apeears at the base of upper stage
5 is found in bore 36040 but not in 30323. None of
the taxa which characterise the younger Weylandites
Zone have been found. Thus the former is upper
stage 5 and the latter lower stage 5b.

These bores are listed in the Appendix and the
distribution of the Permian assemblages is shown on
Pao (i

2. Triassic ?

A unit identified in bores 30323 and 36040 be-
tween Permian and Tertiary (see Figs. 3, 5) failed
to yield any pollen. It is thought, however, that
this unit is an extension of the Triassic found in
the nearby Coorabin Coal Measures (Standing Comm-
ittee on Coalfield Geology, 1978).

3. Early Cretaceous
Early Cretaceous palynostratigraphy follows

Dettmann and Playford (1969) for zonation and
Morgan (1980) for time ranges. The citations of

APPROXIMATE POSITION
OF QUANTITATIVE

MODIFIED ZONES
EVENTS

T. bellus
Zone

<= DNinoflagellates

Early Upper

High Myrtaceae ratios

C subdivision

=a <— Upper WN. flemingii acme Sa

P. tuberculatus Zone
Middle

<= Lower N. flemingii acme

High P. mawsonii ratios

Middle N. asperus Zone

Lower N. asperus Zone

P. tuberculatus Zone

BR subdivision

A subdivision

Foe a Go ae

Middle
N. asperus Zone

Fig. 2 Tertiary palynological zones with the modifications
adopted for this paper.

38

species names may be found in these references.
The two occurrences in this study are very simil-
ar.

Of the gymnosperm pollen, Podocarpidites spp.
are the most common, with Alisporites spp.,
Araucariacites australis and Microcachryidites
antarcticus frequent. Classopollis cf C. class-
oides and Ginkgocycadophytus nitidus are infreq-
uent. There is a rich spore flora with Baculat-
isporites comaumensis and Stereisporites antiqua-
sporites the most common. Lycopodiumsporites
spp., Ceratosporites equalis, Cyathidites spp.
and Klukisporites scaberis are seen frequently.
Cicatricosisporites australiensis is present also,
and the presence of Dictyotosporites speciosus
and Pilosisporites notensis place these assembl-
ages in the Dictyotosporites speciosus Zone of
Neocomian-Aptian age (Dettmann and Playford, 1969)
or Aptian-early Albian (Morgan, 1980).

Both assemblages are non-marine with abundant
pollen and plant cellular debris. No dinoflagell-
ates have been found, although there are a few

HELENE A. MARTIN

of the acritarch Micrhystridium sp. in bore 36261.

The bores are listed in the Appendix and the
distribution of the Early Cretaceous is shown on
Fag. ds

4. Tertiary

Palynostratigraphy follows Stover and Partrid-
ge (1973) with some modifications. The P. tuber-
culatus Zone has been modified by the method in
Martin (in press a). The citation of species
names follows Stover and Partridge (1973).

The oldest Tertiary assemblages fit the Mid-
Late Eocene Lower N. asperus Zone, similar to
those reported in Martin (1977). Almost twenty
species whose ranges terminate at the top of this
zone are found here, and any one assemblage may
contain up to eight of them. The zone may be
divided into an older and a younger part, based on
the presence of Triorites magnificus in the latter
(Stover and Partridge, 1973). Partridge (1976)
and Stover and Partridge (1982) use this sub-

cA A Subdivision

Middle

WN. asperus
ZONE

coal

Earty Permian
Stage 3b

Permian Stage 3a

Permian (Upper Stage 5)

A!
25394
30320
36275 36040 :
A 30362 :
30479 30383 36229 d Procene
36331
T bellus ZONE
: P tuberculatus
>| P tuberculatus ‘ ZONE
ZONE B Subdivision
ene aati Pret bee ee ie bacthias A Subdivision | Middle
C Subdivision } C Subdivision |: yone’’s
?Grante
C Subdivision Slate
B Subdivision
C Subdivision P tuberculatus P (uberculalds
ZONE
- = 8B Subdivision ZONE scale jm
P tuberculatus if
ZONE
B Subdivision ic --- +20
P tuberculaius = B Subdivision G gravel, major component
/ A
ZONE ae Subd eice Q gravel, minor component
40
Bits i Middle [ S,S_— sand
t erculatus
A Subdivision Soaps C,c_ clay
ZONE A Subdivision lege LI sit
D _Dinoflagellates, low frequencies
?? Triassic
Middle DD Dinottageliates, abundant
N. asperus
B Subdivision ONE

<q Palynological sample
| | Basement, ce. older
Bue than Tertiary

[ ] brown, yellow, red,
minor grey

ve
ss | pale grey

| dark grey, carbonaceous

Fig. 3 Cross section ALA from Hay to Narranderra. For location,

see Fig. 1.
2

For ages of the palynological units, see Fig.

PALYNOLOGY OF THE MURRUMBIDGEE AREA By

division to recognise a Middle N. asperus Zone.
They restrict the Lower N. asperus Zone to the
lower subdivision of the original Lower N. asper-
us Zone of Stover and Partridge (1973). The
presence of Polycolpites reticulatus, Proteacid-
ites reticulatus and Triorites magnificus in a
number of Murray Basin assemblages indicate that
they belong to the Middle N. asperus Zone.

The Upper N. asperus Zone, of Late Eocene-
Early Oligocene age, recognised in one bore in
Martin (1977), has not been identified in any
others of the Murray Basin, if the diagnosis of
Stover and Partridge (1973) is followed.

The species whose ranges terminate at the top
of the Middle N. asperus Zone decrease in number

B
36078
36102

sea level
Oo ee coe weceecens

Pliocene”

ZONE
B Subdivision

T. bellus ZONE

T.bellus ZONE QC] A Subdivision

scale (m)
(]

40

G gravel, major component

Q gravel, minor component

S,S sand
Cyc clay
A Subdivision LI sit

<q Palynological sample

Basement, i.e. older
than Tertiary

fia] brown, yellow, red,
minor grey

pale grey

Clay, Shale

aad isiltsione dark grey, carbonaceous

Cross section B-B! from Wakool
through Deniliquin. For
location, see Fig. 1. For ages
of the palynological units,
see Fig. 2.

with successively younger assemblages, until none
remain. As the several species which first appear
at the base of the P. tuberculatus Zone are rarely
seen in this area, the latter is usually identifi-
ed on negative evidence, i.e. lack of Middle wn.
asperus Zone species. Other than the diagnostic
species, there is little difference between the
assemblages of the two Zones. The boundary betw-
een the Middle N. asperus and P. tuberculatus
Zones (Fig. 2) in the Murrumbidgee area is thought
to approximate the Eocene Oligocene boundary.

Stover and Partridge (1973) have divided the
P. tuberculatus Zone into lower, middle and upper,
but their diagnosis of these subdivisions does not
work in this area. The thick sections of P.
tuberculatus Zone have been subdivided using three
taxa showing occasional high frequencies which are
defined by constructing a ratio and empirically
choosing a cut off value to delimit the high rat-
ios. Table 1 lists the taxa, the ratios and the
values of the high ratios used in this study.
This method is explained in detail in Martin (in
press a).

High ratios of P. mawsonii are found in both
the upper part of the Middle N. asperus Zone and
the base of the P. tuberculatus Zone. In this
position, they are thought to approximate the
Upper N. asperus Zone which cannot be identified
on the original diagnosis. Some of the coals of
the Upper WN. asperus Zone in the Gippsland Basin
contain very high frequencies of P. mawsonii
(Stover and Partridge, 1973). High ratios or acme
of N. flemingii occurs in two layers in the P.
tuberculatus Zone, one low down either within the
top of the high P. mawsonii ratios or just above
it, and the other much higher up. It is thought
that the lower N. flemingii acme approximates the
true base of the P. tuberculatus Zone. The high
Myrtaceae ratios start about the level of the
upper N. flemingii acme layer and continue into
the Mid Miocene Triporopollenites bellus Zone.
Polyadopollenites myriosporites first appears in
the beginning of the Miocene. It is rare in this
area, but it has found with the high Myrtaceae
ratios, above the upper N. flemingii acme layer.
Consequently, the upper N. flemingii acme layer
is thought to approximate the Oligocene-Miocene
boundary and the high Myrtaceae ratios are Early
Miocene. These stratigraphic positions of the
high ratios are shown in Fig. 2.

The dinoflagellates Operculodinium centrocarpum,
Lingulodinium machaerophorum, Hystrichokolpoma
rigaudiae and Systematophora placacantha (for
citation of species see Lentin and Williams, 1977)
are found in several bores near Hay. Operculod-
inium centrocarpum is by far the most common, and
all of these species are found in the Miocene
(Deflandre and Cookson, 1955). Dinoflagellates
indicate marine or brackish water, and it is
thought that their occurrence at Hay indicates
the Miocene high sea level, when channels or low
lying areas would have been flooded. For the
southern Australian margin, the peak of the Miocene
marine transgression occurs about the Early-Mid
Miocene boundary (Loutit and Kennett, 1981). The
dinoflagellates are stratigraphically within the
high Myrtaceae ratios, above the upper N. flemin-
gii acme. Their position is thus in agreement with

40 HELENE A. MARTIN

the other palynological events in the upper part
of the P. tuberculatus Zone (see Fig. 2).
tuberculatus Zone has

For convenience, the P.

been divided thus:

high P. mawsonii and lower

N. flemingii acme layer
without high ratios

upper N. flemingii acme layer
and high Myrtaceae.

A subdivision,

B subdivision,
C subdivision,

These subdivisions are shown on Fig. 2 and
their occurrence in the bores are listed in the
Appendix.

The Triporopollenites bellus Zone is identif-
ied by several diagnostic species which first

36373
C 30323

C Subdivision ae

P. tuberculatus
ZONE

P. tuberculatus
ZONE

C Subdivision

P. tuberculatus

Ordovician ?
ZONE

siltstone

B Subdivision

Middle
N. asperus
ZONE

A Subdivision

N. asperus
ZONE

teat scale |[m|

‘:t::} silty sandstone 0
“1 Barren

7Triassic as

40

[| Coal Upper Permian 60
Lower Stage 5b

30348

appear at the base of the zone (Stover and Part-
ridge, 1973). Assemblages of this zone are found
in a few bores. See Appendix.

Pliocene assemblages (Martin, 1973) occur in
only two bores. See Appendix.

DISCUSSION

The Middle N. asperus Zone underlies most of
the Basin. It is, however, lacking from bores
30320, JX-7 and 30497 where the P. tuberculatus
Zone directly overlies the basement. In the first
two bores, the A subdivision of this zone rests
on the basement, whereas in the latter, the B
overlies basement. There is a considerable dis-
placement between the A subdivision of the first

C Subdivision

P. tuberculatus
ZONE

P. tuberculatus B Subdivision

ZONE

C Subdivision :
:| P. tuberculatus

ZONE A Subdivision

B Subdivision te aren

Dictyotosporites

speciosus
== Zone
A Subdivision *
See caption

Middle
N. asperus
ZONE

decomposed granite

q Palynological sample Iq barren]

Basement, i.e. older

G gravel, major component than Tertiary

Q gravel, minor component
S,S_— sand

C,c clay

CJ brown, yellow, red,
minor grey

pale grey
dark grey, carbonaceous

For location, see

Cross section C-Cl from Jerilderie across the Murrumbidgee River.
Fig. 1. For ages of the palynological units, see Fig. 2. *The top sample in the
Dictyotosporites speciosus Zone is a mixed assemblage and contains snecies diagnostic
of the Middle N. asperus Zone. Therefore, this latter zone must be present although
it has not been sampled.

Fug. 5

PALYNOLOGY OF THE MURRUMBIDGEE AREA 4]

two bores and their neighbouring deep bores,
36040 and 30691/36201 respectively (see Figs. 3,
4). This indicates movement along a fault, some-
time after the deposition of the A subdivision.
If the questionable identification of the C sub-
division in 30323 is accepted, then the displac-
ement of this subdivision between this bore and
30497 would suggest that movement along the fault
occurred after the deposition of the C subdivis-
ion (Fig. 5). Unfortunately, this subdivision is
not well developed in the southern and south-
easterly deep bores so the evidence of the precise
timing of movement is inconclusive. The two deep
bores are situated in the Ovens Valiey Graben
(Yoo, 1982), a basement feature and this evid-
ence shows that Tertiary movement has occurred
along one of the basement faults.

The middle N. asperus Zone sediments at
Narrandera occur in a narrow valley a few kilo-
meters upstream from the Basin margin. This long,
narrow embayment extended into the highland flan-
king the Eocene plain and is the earliest recog-
nisable stage of the Murrumbidgee River System
(Woolley, 1978). The Early-Mid Miocene dinoflag-
ellates at Hay probably may mark another, but
later, embayment of the Murrumbidgee River, which
became flooded by the rising sea level.

It 1s curious that the Upper W. asperus Zone
as described by Stover and Partridge (1973) can-
not be identified in this area. As discussed
previously, there is a gradual change from the
Middle N. asperus to P. tuberculatus Zones in
successive assemblages, and apart from the diag-
nostic species, the assemblages of the two zones
are very similar. It is thought that the A sub-
division with the high P. mawsonii content, which
is the only character in agreement with the orig-
inal description of the Upper W. asperus Zone,
might be the time equivalent (more or less) of
the one occurrence of this zone, found further to
the west (Martin, 1977). An alternative explan-
ation is non-deposition in the Murrumbidgee area
during the time of the Upper WN. asperus Zone.
This possibility is considered unlikely, since
the latest Eocene - earliest Oligocene was a time
of high sea level (Loutit and Kennett, 1981).

The three quantitative events used here to
subdivide the P. tuberculatus Zone are based on
taxa which form a palaeoecological series: P.
mawsonii in the wettest habitat, WN. flemingii
intermediate, and Myrtaceae in the driest (Martin,
in press a). The sediment type associated with
the high ratios and the ecology of the living

taxa both confirm this series (Martin, in press a).

The degree of wettness may be controlled by clim-
ate and/or hydrology, i.e. the efficiency of
drainage. Thus the high P. mawsonii ratios ind-
icate more swampy conditions and the two N.
flemingii acme layers periods of improved drain-
age. The high Myrtaceae ratios indicate the start
of a climatic change which heralds the beginning
of the trend to aridity and which continues into
the Mid-Late Miocene and is associated with the
disappearance of Nothofagidites and the rise to
dominance of Myrtaceae (Martin, 1982).

If the quantitative events and their strat-
igraphic positions (see Fig. 2) are compared with
the sedimentary cycles for the southern margin of

Australia (Loutit and Kennett, 1981) there is a
reasonable correspondence. High sea levels in
latest Eocene time correspond to the high P.
mawsonii ratios. Drainage would have been very
inefficient at this time with a consequent increase
in swampy habitats conducive to P. mawsonii. There
is a large drop in sea level, with the lowest level
in Early Oligocene time corresponding to the lower
N. flemingii acme. Lowered sea levels would have
created better drainage. Sea levels rise through-
out the Oligocene, but there is a minor drop to a
lower level about the Oligocene-Miocene boundary,
corresponding to the upper N. flemingii acme. Sea
levels rise further to their highest levels about
the Early-Mid Miocene, when the low lying areas at
Hay were flooded, creating the habitats for dino-
flagellates. No doubt the terrestrial environment
became more swampy, but P. mawsonii does not
increase in abundance, for the climate had become
drier. The swamp habitat was probably occupied

by species of Myrtaceae which tolerate a much
drier climate.

It is suggested that changing sea levels have
largely controlled the stratigraphic distribution
of the high ratios through the Oligocene. However,
the Murrumbidgee area is a special case, for the
same high ratios are identified in the Lachlan area
but they do not show the same patterns as those of
the Murrumbidgee (Martin, 1984).

If eustatic changes have had such an influence
on the palynology then one may expect them to have
had an influence on sediment deposition and pres-
ervation as well. As discussed previously, the
further the distance from the sea, the less marked
the effects of eustatic changes. The Mid Oligoce-
ne hiatus shown in the interpretation of the Murray
Basin by Brown (1983) is not recognisable here.
There is no evidence in the palynology to suggest
a hiatus either. Subtle changes, however, such as
the raising or lowering of the water table by a
few metres would make a great difference to plant
growth. Thus although the influence of eustatic
changes is not recognisable in the sedimentary
record, it registers in the palynologic record
through changes in the relative abundance of the
pollen types.

The failure to recover pollen from most samp-
les above 100m is striking. Simple lack of depo-
sition and/or erosion is unlikely to be the cause
of this failure for there is 100m of sediment
above the level of the pollen bearing deposits. It
is thought that the climate had become too dry to
support an abundance of the permanently wet sites
required for pollen preservation. The occasional
occurrence of the T. bellus Zone and Pliocene
assemblages are viewed as representing an occasion-
al body of permanent water in the landscape of the
time. The permanently wet sites started decreas-
ing during the subdivision of the P. tuberculatus
Zone, were much reduced by the time of the T.
bellus Zone and extremely rare in the Pliocene.
The frequency of permanently wet sites in a land-
scape is largely dependant on rainfall, either
over the area itself or the catchment that feeds
it. By the same token, if the rainfall is in-
sufficient to support widespread permanently wet
sites, the climate is dry enough to allow cycles
of wetting and drying which are most destructive
to pollen. Under such circumstances, pollen

42 HELENE A. MARTIN

preservation would require rapid burial, to depths

beyond the fluctuating water table, an unlikely
proposition given the generally low rates of

sedimentation in this area (R.M. Williams, pers.
comm. ).

TABLE 1.

Selected taxa showing occasional high frequencies and the definition of

high ratios.
press a).

Taxon
Phyocladidites
mawsonii
Nothofagidites
flemingii

Myrtaceae

For a full explanation of the method, see Martin (in

High ratio

P. mawsonii
Total gymnosperms

N. flemingii

Total Nothofagidites

Myrtaceae

Total Nothofagidites

CONCLUSIONS

The palynologic record shows that Tertiary
deposition occurred from Mid-Late Eocene through
Early Miocene time over most of the area under
study. An hiatus corresponding to lowered sea
levels cannot be recognised during this time.
Lowered sea levels, however, have influenced the
palynologic record. Plants require specific
ecologic conditions, and the lowering of the wat-
er table by only a few metres, as would occur
with more efficient drainage during times of low
sea level, could make a great difference to the
vegetation. The quantitative events (high ratios)
of the P. tuberculatus Zone show a reasonable
correspondence with eustatic changes.

Pollen assemblages are only occasionally re-
covered from Mid Miocene time onwards. The clim-
ate had become too dry to support more than an
occasional permanently wet site which is required
for pollen preservation.

ACKNOWLEDGEMENTS

I am indebted to the Water Resources
Commission of New South Wales for financial supp-
ort. Mr. R.M. Williams of the Hydrogeological
Section, W.R.C. of N.S.W. has most generously
assisted with background information and discuss-
ion. I wish to thank the referee for invaluable
criticisms of this work.

REFERENCES

BEMBRICK, C.S., 1975. The Murray Basin. In
Markham, N.L. and Basden, H., Eds. The Mineral
Deposits of New South Wales. Geol. Surv.
N.S.W.

BROWN, C.M., 1983. Discussion: A Cainozoic
history of Australia's South east Highlands.
J. Geol. Soc. Aust. 30: 483-486.

DEFLANDRE, G. & COOKSON, I.C., 1955. Fossil micro-
plankton from Australian Late Mesozoic and
Tertiary sediments. Aust. J. Mar. Freshw. Res.
6: 242-313.

DETTMANN, M.E. §& PLAYFORD, G., 1969. Palynology
of the Australian Cretaceous: A review. In
Campbell, K.S.W., Ed. Stratigraphy and Palae-
ontology: Essays in honour of Dorothy Hill.
A.N.U. Press, Canberra.

KEMP, E.M., BALME, B.E., HELBY, R.J., KYLE, R.A.,
PLAYFORD, G. & PRICE, P.L., 1977. Carbonif-
erous and Permian palynostratigraphy in
Australia and Antarctica: A review. B.M.R.
J. Aust. Geol. & Geophys. 2: 177-208.

LAWRENCE, C.R., 1975. Geology, hydrodynamics and
hydrochemistry of the southern Murray Basin.
Geol. Surv. Vict. Mem. 30.

LENTIN, J.K. §& WILLIAMS, G.L., 1977. Fossil
dinoflagellates: Index to genera and species.
Bedford Inst. Oceanog. Rep. Ser. BI-R-77-8.

LOUTIT, T.S. §& KENNETT, J.P., 1981. Australasian
Cenozoic sedimentary cycles, global sea level
changes and the deep sea sedimentary record.
Oceanologica Acta SP. Proceedings 26th Inter-
national Geological Congress. Geology of
Continental Margins Symposium, Paris July 7-17,
1980, 45-65.

PALYNOLOGY OF THE MURRUMBIDGEE AREA

REFERENCES (Cont. )

MARTIN, H.A., 1973. Upper Tertiary palynology in
southern New South Wales. Geol. Soc. Aust.
Spec. Pub. 4, 35-53.

MARTIN, H.A., 1977. The Tertiary palynology of
the Murray Basin in New South Wales. I. The
Hay-Balranald-Wakool Districts. J. & Proc.
Roy. Soc. N.S.W., 119, 41-47.

MARTIN, H.A., 1982. Changing Cenozoic barriers
and the Australian paleobotanical record. Ann.
Missouri Bot. Gdn. 69: 625-669.

MARTINs H.A. (in press a). The use of quantitat-
ive relationships and palaeoecology in strat-
igraphic palynology of the Murray Basin in
New South Wales. Alcheringa.

MARTIN, H.A., 1984. The stratigraphic palynology
of the Murray Basin in New South Wales. III.

The Lachlan area. J. & Proc. Roy. Soc. N.S.W.:

117.

MORGAN, R., 1980. Palynostratigraphy of the
Australian Early and Middle Cretaceous. Mem.
Geol. Surv. N.S.W. Palaeont. 18: 1-153.

PARTRIDGE, A.D., 1976. ‘The geological expression
of eustacy in the Early Tertiary of the Gipp-
sland Basin. APEA Jl., 16: 73-79.

Standing Committee on Coalfield Geology, 1978.
Stratigraphy of Coorabin Coal Measures. Rec.
Geol. Surv. N.S.W., 18: 114-146.

APPENDIX.

Bores are arranged from W to E, then N to S.
See Fig. 1 for location. For the ages of the
palynological zones see Fig. 2. All bores have
been sunk by the Water Resources Commission of
New South Wales except for one, JX-7, a Mines
Administration Pty. Ltd. bore.

36078
76.2 - 77.7m Pliocene
94.4 - 108.2m T. bellus Zone
114.3 - 152.4m C subdivision
155.4 - 250.0m B subdivision bp. tuberculatus
254.5 - 266.7m A subdivision Zone
280.4 - 349.0m Middle N. asperus Zone
30479

109.7 - 135.6m C subdivision, P. tuberculatus
Zone with maximum dinoflagellates
at 112.8-114.3m.

137.1 - 198.1m B subdivision, P. tuberculatus
Zone

36331/36246

1200 2 ivisi
154.0m C subeivision b Laer cree

164.0 - 277.0m B subdivision
Zone

291.0 - 292.0m A busdivision
307.8 - 370.3m Middle N. asperus Zone

43

STOVER, LE. & PARTRIDGE, A.D., 1973. Tertiary
and Late Cretaceous spores and pollen from the
Gippsland Basin, southeastern Australia. Proc.
Re S0Gs VICtC.. 055 25/2287.

STOVER, L.E. & PARTRIDGE, A.D., 1982. Eocene
spore-pollen from the Werillup Formation, Wes-
tern Australia. Palynology 6: 69-95.

WOOLLEY, D.R., 1978. Cainozoic sedimentation in
the Murray drainage basin, New South Wales
section. Proc. Roy. Soc. Vict. 90: 61-65.

WOOLLEY, D.R. & WILLIAMS, R.M., 1978. Tertiary
stratigraphy and hydrogeology of the eastern
part of the Murray Basin in New South Wales.
in Storrier, R.R. & Kelly, I.D., Eds. The
hydrogeology of the Riverina Plain of south
east Australia. Aust. Soc. Soil Sci. Riverina
Branch.

Yoo, E.K., 1982. Geology and coal resources of
the northern part of the Oaklands Basin.
Quart. Notes Geol. Surv. N.S.W. 49: 15-27.

30435
109.7 - 146.2m C subdivision

150.9 - 184.4m B subdivision P. tuberculatus

196.6 - 198.1m A subdivision | 27°
36240
115.8 - 253.0m B subdivision, P. tuberculatus
Zone
326.1 - 335.3m Middle N. asperus Zone
36025/2

105.1 - 106.6m T. bellus Zone
109.7 - 138.6m C subdivision, P. tuberculatus

Zone
30422
109.7 - 155.4m C subdivision, P. tuberculatus
Zone
36211
eas

8 - 137.8m C subdivision P. tuberculatus
147.8 - 195.0m B subdivision Zone
280.4 - 281.9m Mixed A subdivision, P. tubercul-
atus Zone and Stage 3a of the
Early Permian
36069
120.0 - 129.5m C subdivision P. tuberculatus
135.6 - 137.2m B subdivision Zone

a4 HELENE A. MARTIN

25363
125.9 - 129.5m C subdivision | P. tuberculatus
134.1 - 185.9m B subdivision Zone

56201/30691
123.7 - 124.3m Early T. bellus Zone
131.

1 - 138.4m C subdivision Bn, paper eniatae
140.2 - 245.4m B subdivision oe
256.0 - 271.3m A subdivision
274.3 - 323.1m Middle N. asperus Zone
56261

tuberculatus

121.9 - 216.4m B subdivision
Zone

94.5 - 117.3m C subdivision 5
9 :
224.0 - 236.2m A sisvision} :
248.3 - 273.5m Lower N. asperus Zone
278.1 - 289.6m Dictyotosporites speciosus Zone
of the Early Cretaceous

36034

103.6 - 105.1m fT. bellus Zone

106.7 - 132.6m C subdivision, P. tuberculatus

Zone
30883
111.2 - 158.5m C subdivision | P. tuberculatus
164.6 - 178.2m B subdivision Zone
36235
105.2 - 135.6m C subdivision
155.4 = 205.7m B siiivision} Sees ase
210.3 - 243.8m A subdivision
246.1 - 259.8m Middle N. asperus Zone
50443
102.1 - 103.6m Tf. bellus Zone
105.1 - 121.9m C subdivision] P. tuberculatus
123.5 - 207.0m B ate neesy Zone
36229/30362
96.0 - 134.1m C subdivision
137.2 - 185.9m B sinvision} ie emt Cis

193.5 - 230.1m A subdivision
259.1 - 260.6m Middle N. asperus Zone

285m Stage 3b of the Early Permian
30464

O7. Set S4 lim aC Se eee P. tuberculatus

137.2 - 138.7m B subdivision Zone
36275

118.8 - 125.9m C subdivision

148.1 - 185.3m B shiv ision| Pas

214.3 - 238.6m A subdivision

246.3 - 288.9m Middle N. asperus Zone

322.7 - 334.7m Stage 3a of the Early Permian
30959

168.0 - 184.0m B subdivision Zone
36283
142.6 - 144.2m Upper Stage 4a, Early Permian
JX-7 (Mines Administration Pty. Ltd.)
140.2 - 141.7m B subdivisionl P. tuberculatus
149.3 - 158.5m A subdivision f{ Zone
30348
117.3 - 121.9m C subdivision, P. tuberculatus
Zone

130.5 - 156.0m C eee P. tuberculatus

Helene A. Martin,

School of Botany,

University of New South Wales,
P.O... Box 1,

Kensington, NSW, 2033, Australia.

- §89.0m C subdivision
- 140.8m B subdivision

; P. tuberculatus
154.5 - 156.0m A subdivision

if

5

Zone

- 168.2m Middle N. asperus Zone
.om Dictyotosporites speciosus Zone
of the Early Cretaceous

122.0 - 150.0m B subdivision] P. tuberculatus
158.0 - 192.0m A subdivision Zone
198.0 - 221.0m Middle N. asperus Zone

94.0 - 140.0m 8B subdivision] P. tuberculatus
166.0 - 184.0m A Man zone
206.0 - 212.0m Middle N. asperus Zone
36040
109.7-- lll.2m Upper fT. bellus: Zone
128.0 - 195.1m B ee tuberculatus
196.6 - 201.2m A subdivision Zone
216.4 - 237.7m Middle N. asperus Zone
289.6 - 307.8m Upper Stage 5 of the Early Perm-
ian
30323
131.1 - 146.3m ? C subdivision
149.3 - 187.4m B subdivision ie tubercutaeus
192.0 - 204.2m A subdivision ous
211.8 - 239.3m Middle N. asperus Zone
276.0 - 278.0m Barren, ? Triassic
330.7m Lower Stage 5b of the Late
Permian
30497
105.0 - 106.7m C subdivision] P. tuberculatus
108.2 - 152.4m B Subd deiGay Zone
30489
96.0 - 115.8m C subdivision, P. tuberculatus
Zone
36368

136.0 - 138.0m Middle N. asperus Zone

112.8 - 126.5m A subdivision, P. tuberculatus

Zone
25394
32.3 - 55.5m Pliocene
100.6 - 101.2m Upper T. bellus Zone
115.2 - 134.4m B subdivision, P. tuberculatus

Zone
143.6 - 160.6m Middle WN. asperus Zone

Note:

The Narranderra bore in Martin (1973) is 25394.
This report was written before the zonation scheme
of Stover and Partridge (1973) became available
and everything below 100m is incorrectly designat-
ed as Miocene. This report supersedes that in
Martin (1973).

(Manuscript first received 3.1.84)
(Manuscript received in final form 28.4. 84)

Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 45-51, 1984

ISSN 0035-9173/84/010045 — 07 $4.00/ 1

The Stratigraphic Palynology of the Murray Basin in
New South Wales. III. The Lachlan Area

HELENE A. MARTIN

ABSTRACT. The geology and palynology of the Lachlan area of the eastern edge of the Murray
Basin is generally similar to that of the Murrumbidgee area. The oldest Tertiary sediments are

the Mid-Late Eocene Middle Nothofagidites asperus Zone.

The Oligocene-Early Miocene Proteac-

idites tuberculatus Zone may form thick sections which require subdivision. The Mid-Late
Miocene Triporopollenites bellus Zone is not found here. In the southwestern region of the
Lachlan area, the basement is deeper and the sedimentary sequence thicker. Here the P.
tuberculatus Zone may be subdivided using the quantitative events (i.e. high ratios), similar
to that of the Murrumbidgee area. Elsewhere, the pre-Tertiary basement is shallower and the
sedimentary sequence thinner. Here, the quantitative events show different patterns to those
of the Murrumbidgee area. It is thought that better drainage over the shallower basement is

the Tikely cause of the difrerént: patterns.

The two records of basement assemblages are both the Early Cretaceous Dictyotosporites

speciosus Zone.
INTRODUCTION

Tertiary deposition in the Lachlan area (see
Fig. 1) is generally similar to that of the
Murrumbidgee (Martin, 1984). The oldest Tertiary
sediments are the Mid-Late Eocene Middle Notho-
fagidites asperus Zone, like those of the
Murrumbidgee area. The Proteacidites tubercul-
atus Zone may form thick sections also, and the
problems of subdividing them are encountered here
as well. In the Murrumbidgee area, these prob-
lems have been solved by the use of quantitative
events (i.e. high ratios). However, this
solution does not work over most of the Lachlan
area for while the high ratios may be identified,

2.21296

eMossgeil

al

436312
430406

LS
A 36329

Booligal

they do not form similar patterns to those seen in
the former.

This paper presents the stratigraphic palynology
of the Tertiary and basement of the Lachlan area.
The differences between it and the Murrumbidgee
are discussed and the likely causes suggested.

GEOLOGY

The geology of the Murrumbidgee area presented
in Martin (1984) is applicable in general to the
Lachlan area. The discussion below concentrates

\ 36171A
\
30023 |
In \
30022
Cr 25408 \

4
achlan ne
A25403 LC mS

AZo

A30044

A30174

HILLSTON

A30261

A Bore --—-— Fault
A Middle N.asperus Zone @y ___ Margin of Basin
© Early Cretaceous basement

— == Probable limits of Marine Tertiary

20 30 km

Fig. 1 Locality map. The probable extent of the marine Tertiary and the margin of the Basin are from
Bembrick, 1975. The faults are from the 1:250,000 Geological Series, Cargellico SI 55-6.

46 HELENE A. MARTIN

on the differences between the two areas.

The pre-Tertiary basement of the Lachlan is
shallower over most of the area. It deepens to-
wards the south west and the bores in this region
are situated on the Ivanhoe Trough, a basement
feature (R.M. Williams, pers. comm.). As a
consequence of this shallower basement, which
has been relatively shallow throughout the Tert-
iary the section is not as thick as that of the
Murrumbidgee area, with the exception of the
south west region where the section is much
deeper.

The sediments in the Lachlan area are gener-
ally not as carbonaceous as those of the Murrum-
bidgee area. The dark grey clays are not as
common and pale to mid-grey clays may be encount-
ered low down in the sequence. At the top of
the sequence, barren pale grey sediments may
extend above the pollen bearing beds before the
change to brown, yellow, red and minor grey
sediments.

Overall, sands are more common in the Lachlan
area than in the Murrumbidgee area (R.M. Williams,
pers. comm. ).

These differences in the geology are relative-
ly slight but they are thought to be important for

palynology.
MATERIALS AND METHODS

All of the bores have been sunk by the Water
Resources Commission of New South Wales and most
reach basement. The methods are the same as
those described in Martin (1984).

PALYNOSTRAT IGRAPHY
(1) Early Cretaceous.

Early Cretaceous assemblages are found in two
bores and palynostratigraphy follcwsDettmann and
Playford (1969) for zonation and Morgan (1980)
for time ranges. The citations of all species
below follow these references. All of the ass-
emblages are similar. The gymnosperms Microcach-
ryidites antarticus and Podocarpidites spp. are
the most common. Araucariacites australis is

Late

Age :
g Neocomian

Zones

Morgan (1980) C. stylosus

Zones
Dettmann §& Playford (1969)

Dictyotosporites speciosus

D. filosus

Dictyophyllidites crenatus

Trilobosporites trioreticulatus

Fig. 2
§& Playford (1969).

D. speciosus

The time ranges of Early Cretaceous diagnostic species.

relatively abundant and Alisporites spp., Ginkgoc-
ycadophytus nitidus, and Classopollis of C. class-
oides are present also. There is a rich spore
flora of Cyathidites spp., Lycopodiumsporites
spp., Leptolepidites spp., Baculatisporites com-
aumensis, Stereisporites antiquasporites and
others. Four diagnostic species are present and
their ranges are shown on Fig. 1. The ranges of
Morgan (1980) are preferred for they are based on
more comprehensive data than that of Dettmann §
Playford (1969). Thus these assemblages fit the
Dictyotosporites speciosus assemblage of Aptian
into early Albian age (Morgan, 1980).

All of the assemblages contain abundant plant
debris. No dinoflagellates have been found in
Bore 36342, indicating wholly non-marine environ-
ments. A few dinoflagellates have been found in
Bore 36321. Several species are present, but
usually only one specimen of each. Most are
broken or lack the definitive diagnostic features
so reliable identification is not possible. How-
ever, the distinctive genus Odontochitinia which
is known from the D. speciosus Zone (Morgan, 1980),
is present. These few dinoflagellates indicate
near shore conditions, perhaps the head of an
estuary. The bores are listed in the Appendix and
the distribution of the Early Cretaceous basement
is shown on Fig. 1.

(2) Tertiary

For the main part, Tertiary palynostratigraphy
follows Stover and Partridge (1973) with the mod-
ifications adopted in Fig. 2 of Martin (1984). The
citations of species names follow Stover and Part-
ridge (1973).

The oldest Tertiary assemblages found here are
placed in the Middle Nothofagidites asperus Zone
of Mid-Late Eocene age, similar to those of the
Murrumbidgee area (Martin, 1984). Its distribut-
ion is restricted, as shown on Fig. 1.

The Late Eocene-Early Oligocene Upper W. asp-
erus Zone, as described by Stover and Partridge
(1973) has not been found in this area. Once the
species restricted to the Lower N. asperus Zone
disappear, the assemblages are those of the
Proteacidites tuberculatus Zone. The Lachlan area
is similar to the Murrumbidgee in this respect.

D. speciosus C. paradoxa

C. paradoxa

meee eee

Solid lines, time ranges from Dettmann

Broken lines, time ranges from Morgan (1980).

PALYNOLOGY OF LACHLAN AREA 47

The P. tuberculatus Zone of Early Oligocene
through Early Miocene age is found in almost
every bore, sometimes in thick sections. The
subdivisions of the P. tuberculatus Zone describ-
ed by Stover and Partridge (1973) cannot be
recognised on their diagnosis, but some sub-
division of these thick sections is necessary.
Three quantitative events have been used to sub-
divide the thick sections of the P. tuberculatus
Zone in the Murrumbidgee area and their strat-
igraphic position is shown in Fig. 2 of Martin
(1984). The same quantitative events are recog-
nised in the Lachlan area, but their stratigra-
phic positions show some differences, viz:

1) High Phyllocladites mawsonii ratios in the
base of the P. tuberculatus Zone in the Murrumb-
idgee area are not found in this position in the
Lachlan area, with the exception of one bore on
the basin edge.

2) High Nothofagidites flemingii ratios may not
form two distinct layers here, as it does in the
Murrumbidgee area. In many bores, high ratios
may be found more or less continuously through
the P. tuberculatus Zone, or sporadically,

30418

C Subdivision

ZONE

P. tuberculatus

ZONE

?Siltstone

Mudstone

Fig. 3 Cross section rear

‘2:11 B Subdivision
P. tuberculatus

ZONE

Ss
C,c

showing no definite pattern of distribution. In
a few bores, the high ratios are concentrated at
the base of the zone.

3) High Myrtaceae/Nothofagus ratios are not as
common as in the Murrumbidgee area, but most are
found in the top part of the P. tuberculatus Zone,
so they may be used to define the C subdivision
(see Fig. 2 in Martin, 1984). Some high ratios
may be found lower down in the B subdivision. A
few high Myrtaceae/Nothofagus ratios may be found
well down in the P. tuberculatus Zone in the
Murrumbidgee area also, but not as many as in the
Lachlan area.

As a consequence of these differences in
expression of the quantitative events, the three
subdivisions of the P. tuberculatus Zone may be
distinguished in a few bores, they are question-
able in many, and in some bores, the P. tuber-
culatus Zone cannot be divided at all.

There is one occurrence of the Mid- Late
Miocene Triporopollenites bellus Zone in the most
easterly bore. Older assemblages do not occur
here. Pliocene assemblages are found above the

A!

30417 30416

P. tuberculatus

sea level
P. tuberculatus
ZONE
Middle
N. asperus
ZONE

ARSENY ooh

scale(m) Shale

C
20
Slate
Sandstone 40

<q Palynological sample (< barren)

Basement, i.e. older
than Tertiary

G gravel, major component C] brown, yellow, red,

minor grey
Q gravel, minor component
pale grey
sand
clay dark grey, carbonaceous

For location of bores see Fig. 1.

48 HELENE A. MARTIN

T. bellus Zone.

No dinoflagellates have been found in the
Tertiary. This deposition is entirely non-marine.

The distribution of the zones and their sub-
divisions in the bores are listed in the Appendix.
Three cross sections are shown in Figs. 3-5.

DISCUSSION

The Early Cretaceous assemblages were probab-
ly deposited at a time of high sea level which
would have induced more swampy conditions on the
land. Some slight influence of the sea is indic-
ated in the most northerly bore which contains a
few dinoflagellates. These deposits would have
been a southerly extension of the Great Austral-
ian Basin.

The Middle N. asperus Zone is not encountered
very often in the Lachlan area. Some may have
been removed by channelling, e.g. Bores 30407
and 30411 (see Fig. 4) where the P. tuberculatus
Zone extends well below the level of the Middle
N. asperus Zone in the neighbouring bores. How-
ever, the basement is somewhat irregular with
highs, e.g. Bores 30410 (Fig. 4) and 36321 (Fig.
5) which would have been above the swampy areas
at the time the Middle N. asperus Zone was being
deposited. The topography need not have been
more than a few metres.

B 36304

C Subdivision C Subdivision

B Subdivision

P. tuberculatus
ZONE

P. tuberculatus
ZONE

B Subdivision

P. tuberculatus

ZONE N. asperus

B Subdivision ZONE

ae Phyllite

M
N. asperus
ZONE.

Siltstone

scale (m)

Phyllite

60

Siltstone and
Sandstone

Fig. 4 Cross section BoB. For location of bores see Fig. 1.

P. tuberculatus

Middle
N. asperus
ZONE.

Phyllite

The Upper N. asperus Zone as described by
Stover and Partridge (1973) is not found here,
Similar to that of the Murrumbidgee area. The high
P. mawsonii ratios in the latter are thought to be
the time equivalent of this zone (Martin, 1984).
However, these high ratios are not found in the
Lachlan area hence the identification of any time
equivalent is impossible. As the Upper W. asperus
Zone was a time of high sea level its preservation
is expected. It is thought that the shallower
basement coupled with more sands and a greater
irregularity of the terrain produced better drain-
age so that the swampy environment required by P.
mawsonii was insufficient to produce the high
ratios. The general lack of carbonaceous sedim-
ents when compared with the Murrumbidgee area
supports this interpretation.

The diffuse nature of the high WN. flemingii
ratios, running through most of the P. tubercul-
atus Zone is the most striking difference when
compared with the Murrumbidgee area. This differ-
ence is not seen in the three southern-most bores
where the basement deepens. Here the P. tubercul-
atus Zone may be divided into the three subdivisio-
ns used in the Murrumbidgee area. Elsewhere, over
the shallower basement, the better drainage would
have been conducive to N. flemingii high ratios
through most of the P. tuberculatus Zone, so that
they are not confined to the times of lowered sea
levels. This interpretation based on the differ-
ence in drainage is in accord with that for

S040 30411 30414 30416

P. tuberculatus
ZONE

!] P. tuberculatus

P. tuberculatus
ZONE .

P. tuberculatus
ZONE

Middle

Sandstone N. asperus
ZONE

and Granite

Phyllite
Sandstone

<q Palynological sample (<{ barren)
Basement, i.e. older
than Tertiary
G gravel, major component
Q_ gravel, minor component
S,s sand

C,c_ clay

(] brown, yellow, red,
minor grey

f:-4 pale grey
Ged

{A dark grey, carbonaceous

*The palynology of bores 30407 and 30408

is almost identical but the lithology is different, especially in the distributions of the sands.

The log of 30407 is presented here.

PALYNOLOGY OF LACHLAN AREA 49

P. mawsoniil.

In the Murrumbidgee area, the greatest thick-
ness of any N. flemingii acme is 30m. There is
only one occurrence of this thickness and all the
rest are 20m or less. The lower N. flemingii
acme, where it occurs, only consists of one sample,
so the total thickness of the two N. flemingii
acmes combined approximate the thicknesses above.
In the Lachlan area, N. flemingii high ratios may
be found through a thickness of up to 60m. There
are two occurrences of thickness and a number are
greater than 30m. Thus the total thickness of
N. flemingii high ratios in the Lachlan area is
up to twice that of the-Murrumbidgée area. This
evidence supports the interpretation that the wN.
flemingii high ratios in the Lachlan are not the
strict time equivalent of the N. flemingii acmes
in the Murrumbidgee, and that they are found in
the time equivalent of the B subdivision which
occurs between the two acmes of the latter area.

The Mid-Oligocene hiatus of the Murray Basin
(Brown, 1983) cannot be recognised here (R.M.
Williams, pers. comm.), similar to that in the
Murrumbidgee area. The palynologic evidence does
not suggest an hiatus either. The subdivision of
the P. tuberculatus Zone using quantitative events
relies on the ecologic requirements of the selec-
fed specres, The difference in habitat, viz.
better drainage accounts for the observed

36321 36284

214 C Subdivision

P. tuberculatus

P. tuberculatus ae ZONE

| P tuberculatus ZONE B Subdivision

ZONE

EARLY
CRETACEOUS

Siltstone

2?Siltstone

Fig. 5 Cross section eo",

differences when compared with the Murrumbidgee
area.

The high Myrtaceae/Nothofagus ratios, diagnos-
tic of the upper part of the P. tuberculatus Zone
are found consistently in the deeper, southern-
most part of the area where the C subdivision is
clearly identified. Elsewhere, the distribution
is patchy and probably represents small, isolated
swamps. This contrasts with the Murrumbidgee area
where the C subdivision is well represented over
most of the area. Thus the thinner C subdivision
is in keeping with the whole sequence being thinner.

The T. bellus Zone is not found in the Lachlan
area of the Murray Basin itself, unlike that of the
Murrumbidgee area. There is one occurrence in Bore
36171 (see Fig. 1), but it is well beyond the
eastern limits of the Basin edge. Older sediments
do not occur here. There is one occurrence of
Pliocene assemblages in the same bore.

There is a barren section above the pollen
bearing beds, similar to that of the Murrumbidgee
area. However, it is thinner, about 80m in
thickness compared with 100m in the latter, and
this is in accord with the whole sequence being
thinner. The likely reasons for this section being
barren are probably the same as those for the
Murrumbidgee area (Martin, 1984).

Cc!
25408

g
Cc

P. tuberculatus Ce
ZONE

P. tuberculatus

ZONE

Y A Subdivision

P. tuberculatus G gravel, major component

ZONE Q gravel, minor component
S,s sand
C,c clay
ace y <q Palynological sample (<j barren)

Basement, i.e. older
than Tertiary

20
el brown, yellow, red,
minor grey
40
pale grey

dark grey, carbonaceous

For location of bores see Fig. 1.

50 HELENE A.

CONCLUSIONS

The palynologic record shows that Tertiary
deposition occurred from Mid-Late Eocene into
Early Miocene time, and this is similar to that
of the Murrumbidgee area. The Lachlan area may
be divided in two:

1) The southwestern part where the basement deep-
ens and the sedimentary sequence is of a compara-
ble thickness to that of the Murrumbidgee area.
The P. tuberculatus Zone may be subdivided in a
Similar way also.

2) Elsewhere, the basement is shallower and the
sedimentary sequence thinner. Here the quantit-
ative events (i.e. high ratios) of the P. tuber-
culatus Zone show different patterns to those seen
in the Murrumbidgee area. It is thought that
better drainage is the cause of the difference.

Pollen assemblages are not recovered from Early
Miocene time onwards, similar to that in the
Murrumbidgee area. The barren section is thinner
over the shallower basement.

ACKNOWLEDGEMENTS.

I am indebted to the Water Resources Commiss-
ion of New South Wales for financial support of
this work. Mr. R.M. Williams of the Hydrogeolog-
ical Section, W.R.C. of N.S.W. has generously
assisted with background information and critical
comment. I wish to thank the referee for inval-
uable criticisms of this work.

REFERENCES

BEMBRICK, C.S., 1975. The Murray Basin. In
Markham, N.L. & Basden, H., Eds. The Mineral
Deposits of New South Wales. Geol. Surv. N.S.W.

APPENDIX

Bores arranged W to E then N to S. For loc-
ation, see Fig. 1. For the age of the palynolog-
ical zones, see Fig. 2 in Martin (1984). All
bores have been sunk by the Water Resources
Commission of New South Wales.

21296
71- 90m C subdivision, P. tuberculatus Zone
114-115m P. tuberculatus Zone
36321
122-134m P. tuberculatus Zone
144-148m Mixed P. tuberculatus Zone and Early
Cretaceous
152-190m Dictyotosporites speciosus Zone of the
Early Cretaceous
36342
84-100m C subdivision
122-230m B subdivision P. tuberculatus Zone
236-248m A subdivision
262-266m Middle N. asperus Zone
270-286m Dictyotosporites speciosus Zone of the
Early Cretaceous
36296
78- 80m C subdivision, P. tuberculatus Zone
122-184m P. tuberculatus Zone

MARTIN

REFERENCES (Cont. )

DETTMANN, M.E. & PLAYFORD, G., 1969. Palynology
of the Australian Cretaceous: A review. [In
Campbell, K.S.W., Ed. Stratigraphy and Palaeo-
ntology: Essays in Honour of Dorothy Hill.
A.N.U. Press, Canberra.

MARTIN, H.A., 1977. The Tertiary Palynology of
the Murray Basin in New South Wales. I. The
Hay-Balranald-Wakool Districts. J. & Proc. Roy.
Soc. N.S.W. 119: 41-47.

MARTIN, H.A., in press a. The use of quantitative
relationships and palaeoecology in stratigraph-
ic palynology of the Murray Basin in New South
Wales. Alcheringa.

MARTIN, H.A., 1984. The stratigraphic palynology
of the Murray Basin in New South Wales. II. The
Murrumbidgee Area. J. & Proc. Roy. Soc. N.S.W.:
TINT op

MORGAN, R., 1980. Palynostratigraphy of the Aust-
ralian Early and Middle Cretaceous. Mem. Geol.
Surv. N.S.W. Palaeont. 18: 1-153.

STOVER, L.E. §& PARTRIDGE, A.D., 1973. Tertiary
and Late Cainozoic spores and pollen from the
Gippsland Basin, south-eastern Australia. Proc.
R. SOG. Vict. 652) 23/-2872

36284

136-188m P. tuberculatus Zone
36329

70-106m C subdivision

112-178m & subdivision °° "8O°#C teas Zone
36312

78- 80m C subdivision

86-212m B subdivision
36304

70- 98m C subdivision

104-182m B subdivision

190-214m Middle N. asperus Zone
30416

62-130m P. tuberculatus Zone

P. tuberculatus Zone

P. tuberculatus Zone

138-148m Middle w. asperus Zone
30417

74-146m P. tuberculatus Zone
30418

84- 90m C subdivision

134-219m B subdivision
30415

118-120m P. tuberculatus Zone

124-174m Middle N. asperus Zone
30414

86-114m P. tuberculatus Zone

132-142m Middle N. asperus Zone

P. tuberculatus Zone

14970
76- 77m
30411
108-140m
30410
74-120m
30409
108-158m
164-184m
30408
94-138m
30407
102-220m
30406
88- 89m
96-148m
156-162m
168-194m
50405
90-156m
30158
72- 74m
30157
84- 87m
30046
103-149m

PALYNOLOGY OF LACHLAN AREA >)!

P. tuberculatus Zone
P. tuberculatus Zone
P. tuberculatus Zone

P. tuberculatus Zone
Middle N. asperus Zone

P. tuberculatus Zone
P. tuberculatus Zone
C subdivision
B subdivision

? A subdivision
Middle N. asperus Zone

P. tuberculatus Zone

P. tuberculatus Zone
P. tuberculatus Zone
P. tuberculatus Zone

P. tuberculatus Zone

Helene A. Martin,
School of Botany
University of New South Wales,

P.O. Box 1,

Kensington, NSW, 2033, Australia

30044

70- 72m
30174

96- 97m
30261

70- 73m
30023

76- 88m
30022

74- 83m
25408

74- 98m

98-103m
25403

74-107m
30111

56- 64m
30109

69- 79m
36169

23- 70m
36171

61-73m

78- 79m

P. tuberculatus Zone
P. tuberculatus Zone
P. tuberculatus Zone
P. tuberculatus Zone
P. tuberculatus Zone

P. tuberculatus Zone
A subdivision, P. tuberculatus Zone

P. tuberculatus Zone
P. tuberculatus Zone
P. tuberculatus Zone
Pliocene

Pliocene
Late T. bellus Zone

(Manuscript first received 3.1.84)
(Manuscript received in final form 28.4.84)

Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 53-62, 1984

ISSN 0035-9173/84/010053 — 10 $4.00/ 1

Computation of Reaction Matrix Parameters by Perturbation Theory

J. L. Cook, E. K. ROSE AND B. E. CLANCY

ABSTRACT.

The forward problem of computing phase shifts, or the equivalent reaction matrix
parameters, directly from an interaction potential is investigated.
theory provides an excellent way to compute the parameters to high accuracy.

Ordinary perturbation
A quadrature

scheme is given which allows the computation of high orders of the interaction matrix. The
scheme takes into account rapid oscillations in the wave functions at high orders and agrees

well with test cases where analytical results are derived.

Finally, a wide range of interior

potentials in the s-wave case is considered and analytic results are given for the inter-

action matrix.
INTRODUCTION

There is an extensive literature on methods
for solving the inverse scattering problem.
Attempts to determine a local or non-local poten-
tial that reproduces these data have been based on
a knowledge of the scattering phase shift. Most
approaches are very formal and a general review of
these methods has been given by Chadan and
Sabatier (1977). In a paper by Hartt (1980), the
new technique of using Padé approximants to com-
pute the scattering function F = k cota, where a
is the phase shift, has been used formally to
solve both the forward and inverse problem for
nucleon-nucleon scattering. Cook (1972) employed
a much older method in which the intermediate cal-
culation of reaction matrices, which are essen-

tially Padé approximants, were used to solve the
inverse problem. Despite an extensive litera-
ture search, we were unable to locate any recent
publications on the solution to the forward prob-
lem with the aid of reaction matrix parameters.
Such calculations are important to understand

the behaviour of overlap and interaction matrices.

For a review of reaction matrix theory we
refer the reader to the article by Lane and Thomas
(1958). In our discussion of the interaction and
overlap matrices, we use the notation of Cook
(1972). The purpose of this paper is to establish
the connection between perturbation series
(Newton 1966) and the reaction matrix. The usual
Born approximation fails at energies close to a
bound state energy or a resonance pole energy.

On the other hand, the reaction matrix formalism
remains valid, no matter what the size of the
coupling constant might be or how close the energy
is to the bound state or resonance poles. This

led us to surmise that it may be possible to cal-
culate the poles and residues of the reaction
matrix directly from the series. We discovered a
set of recurrence relations for the nt" order over-
lap matrix and energy eigenvalue which relates them
to lower orders of the same quantities. In terms
of numerical computation, this has afforded a very
rapid means of computing the reaction matrix para-
meters up to high orders of perturbation.

We tested the method by applying it to a com-
putation of poles and residues of the reaction
matrix for the n-p system in the triplet s-state.

The correct binding energy was obtained using
Yukawa, Gaussian, exponential and square well
nuclear potentials with coupling constants and
shape parameters derived from the effective range
approximation (Preston, 1965). Heaviside units
are used with the nucleon mass unit throughout
this paper.

We also discuss general power law potentials
and the Woods-Saxon potential in the s-wave case.
A quadrature scheme is derived which allows
accurate computation of overlap and interaction
matrices for high order harmonics, in which the
Bessel function components oscillate very rapidly,
so that ordinary integration schemes do not work
adequately.

A big advantage of reaction matrix theory over
optical model theories is that the behaviour of a
many-channel s-matrix can be investigated using the
old theory of Wigner and Eisenbud (1947). We are
evolving a theory based on this early work that
should prove suitable for pion-nucleon reaction
channels and should also permit the determination
of interaction potentials in non-elastic pion and
associated production channels. A further advant-
age of reaction matrix theory is that it permits
an excellent local energy approximation to the
scattering matrix. Truncation of the sum over
poles in the reaction matrix leads to an acceptable
accuracy in restricted regions; this is always
limited by the fact that all data have to be fitted
over restricted energy ranges.

The general philosophy of the reaction matrix
approach is that Wigner-Eisenbud theory always
allows for real internal wave functions and poten-
tials which are analytically decoupled from channel
to channel. It can be shown formally that such a
scheme will allow only the real part of the scat-
tering phase shift above inelastic thresholds to be
used independently to compute a decoupled inter-
action. This work has been reported by Clayton
(1972). Relativistic corrections can be incor-
porated in the effective interaction.

PERTURBATION. THEORY
The derivation of the first two orders follows

closely that given by Schiff (1949). For the
reaction matrix eigenfunctions U, (x), the total

34

Hamiltonian H is introduced which, in the presence
of an interaction gV(r), satisfies:

HU, (r) = kiU, (2) (1)
and H = Hotsv (2)

where Hy is the free particle Hamiltonian satisfy-
ing

= 2
HW 2) eee)
2
H =. 3° , £+1) (3)
¢ or? r?

and W,,(r) are free particle eigenfunctions with
V = 0 and the same boundary conditions. The over-
lap matrix for a force of range a is defined as

a
Ba = I dr U, (2)W (2) (4)

We now expand U , (7) into a perturbation series of
the form

U(x) = W(x) + 1 gu! (r) (5)

where yp es is the nt ne order perturbation to

U, (r). Hence, from equation (4) we find
ee)
By, = Jy 2 By (6)
and
u™ (x) = XL Bw (r) : (7)

Similarly, ki is the position of the pole in the
reaction matrix R(k*), i.e.

2 Uy (a)
1
R(k?) == } (8)
=O. kj -k*
so we expand ky into a similar series
2 _ y2 np, (n)y?
ki = Ki + » g (k, as (9)

We substitute equations (9) and (5) into equation
(1) and get

aren 1 gnu] =

= ae 0) ']| 5;

my] (10)

and equate corresponding coefficients of ee For
example:

(a) Coefficients of g°

ces = aoe ; (11)
that is
(0) _ (0)
Ce a es cae

J. L. COOK AND OTHERS

(b) Coefficients of g

Hu avw, = Kult) (KOE) AW, (12)

o 2X r
which yields

HBy MW +W, = K2 BW (KU Vw, aa)

Multiplying by W, and integrating over the range
0 < r < a, we use the orthonormal property of Wy
to get

: GQ) 2 AU
(i) Ba = eae for A # u
r
(ip (KXY)* =v, (14)
a
(iii) Vin = | dr V(r)W, (r)W, (x)

Oo

As in Schiff's derivation, we substitute equation
(5) into the orthonormal conditions

a
(i) | dr U, (r)U,, (1) = 8).

fe)
(15)
a
ii dr W W = 6

(44) iE rW(r)W (x) = 6,

and obtain for the coefficient of g
pil)
By, = 0 : (16)

(c) Coefficients of g?

V,5V
2) Sl | Oe
(i) Bau = i “12 2 “2 ) B By vs for \ # u
(ix) Bt2? = 7) [eee ee (17)
dAMP EAD,

(c) Coefficients of g?

i ee ee j pl2)y +(k cae ate ‘

Bu K2-K2 AY VU
u
+ ("a> | for Az7uU
(ii) B®) - 2) BB (18)
2
iA) 0) = 2 PY O)"B ae

By Jeates increasing orders of n, we find
the general recurrence relations:

COMPUTATION OF REACTION MATRIX PARAMETERS 55

(aes, Sra (p) ,(n-p)
(ii) B ee) B= B ‘
AA 2 p oy Au AU
(19)
feng) es YB y ‘y aia sie 2

Thus we have a method for calculating B, the U, (a)
and kj which determines R(k? ). The Beacceniny
phase shifts are then found from the relationship
(Preston 1965):

s(q?) = o7f8(Q") «of ERG DOB) (20)

where Q is the hard sphere phase factor, | L = stip,
8(q2 ) is the scattering phase shift, s(q? ) and
p(q?) are the level shifts and penetration factors
respectively, as completely tabulated by Lane and
Thomas (1958) and by Preston (1965), and B = -2&,
where % is the orbital angular momentum of the par-
tial wave considered.

COMPUTATIONS

The definitions of W yp) for free particles in
an s-state yield

(i) W(t) = /% sin(ue} Le
(ii) W (a) = é (-1)" en
Gi) Ket.

We now consider the four potentials fitted by
Preston to the n-p system in the triplet state.

(a) The Yukawa Potential
-r/r

n
e

gVv(r) = (22)

r
which, when substituted into equation 14 (iii),
gives for large a (Gradshteyn and Ryzhik 1965):

a*+(Atutl nore
Fp etic ave eee 1
a*+(A-u)?n? xt

(i) V

i
Au 2a

ii

(44) g = Gr,

where G is the dimensionless coupling constant.
Preston's parameters give:

g = -0.3330 , fis 7.595 :

We varied the value of 'a' for the calculation
of By Poa , (a) and k? to study the convergence of
the ABried and found that 'a' must be large enough
for equation (23) to be valid. On the other hand,
since the convergences became slower as 'a'
increased, we settled for a value around 'a' 50 to
satisfy the criterion V(a) < 0.01 kes which
required the maximum value of n = N °v90. This com-
putation took less than half a minute on the AAEC's
IBM3031 computer. From equation (2) we, see that
the poles of the s-matrix, denoted by q? » occur
when .

R(q5) (L(qy)-B) = 1 (24)

The values of U, (a); ky and qs are shown in Table 1.

For the triplet s-state
L = -la,la 5 ‘B= 0

and ;
10 U2 (a)
‘
lal ) ae (25)
=0 k+lqUl

This is the most difficult case in which to
obtain suitable convergence, but the convergence
rate improves rapidly as A increases and, for the
10th order, N = 3 is satisfactory for both Uio (a)
and are The convergence is always slowest for
A = 0. Nevertheless, it is important to determine
U, (a) and k} accurately, since the value of U, (a)
comes close to W, (a) when the cut-off radius is
large, and round-off can occur when the scattering
matrix is calculated, owing to cancellations
between © and the multiplying term.

(b) The Gaussian Potential
We use
-(r/r,,)*
CVU) aa age (26)

For this case

ae a oa
ve =e Vn [exp] --w9 1? =
nr
- exp|-Qvuel)? 2 || (27)
4a?

and Preston's parameters are:
g = -0.07727 , Ee 7.003

Satisfactory convergence was obtained for
a v20 and N, the maximum required order, about 13;

the values are listed in Table 2. The discrep-
ancies are more likely due to the errors in the
effective range approximation, which we estimate
to be at least 10%. Naturally, we could obtain a
perfect fit to q, by varying our parameters, but
we chose to compare the two methods.

(c) The Exponential Potential
The potential is:
t/t.
gV(r) = ge (28)
with parameters
g = -0.2016 A = S195

The resulting interaction matrix is:

1
Voge at |=— - ae | (29)
ML ars (A-n)?n?r? 0 a?+(Atutl) ?m Boe

Suitable convergence was achieved with a 30 and
N «40. The reaction matrix parameters are shown
in Table 3.

(d) The Square Well Potential

This satisfies

J. L. COOK AND OTHERS

TABLE 1
REDUCED WIDTHS AND POLES OF THE R-MATRIX FOR THE
n-p SYSTEM WITH THE YUKAWA POTENTIAL

x U, (a) KY qe (calc)
0 0.0837 -2.565 x 1073 -2.418 x 1073 +10%
i -0.3187 2.839 x 1073

2 0.2294 12655.1x. LOT

3 -0.2137 35870 Xi Ou

4 0.2085 6.905 x 1072

5 -0.2051 0.1075

6 0.2042 0.1540

7 -0.2025 0.2085

8 0.2027 0.2710

9 -0.2012 0.3414
10 0.2021 0.4198

q2 (experiment) = -2.37 x 1073

TABLE 2
REACTION MATRIX PARAMETERS FOR THE GAUSSIAN
POTENTIAL IN THE n-p SYSTEM

U, (a) ky qe (calc.)

0 0.2263 -4.081 x 1073 -2.179 x 1073 +10%
1 -0.3631 0.03349

2 0.3280 0.1314

3 -0.3223 0.2789

4 0.3199 0.4760

5 -0.3187 On227

6 0.3180 1.0187

7 -0.3176 1.3641

8 0.3173 1.7588

9 -0.3171 2.2029
10 0.3169 2.6964

TABLE 3
REACTION MATRIX PARAMETERS FOR THE EXPONENTIAL
POTENTIAL IN THE n-p SYSTEM

r U, (a) ky qs (calc.)

0 0.1587 ~3.045:x 1073 -2.255 x 107% +10%
1 -0.3217 0.01132

2 0.2746 0.05240

3 -0.2659 0.1166

4 0.2629 0.2033

5 -0.2614 0.3123

6 0.2607 0.4434

4 -0.2601 0.5966

8 0.2598 0.7719

9 -0.2594 0.9691

10 0.2593 1.1883

COMPUTATION OF REACTION MATRIX PARAMETERS oy

ev(r) = Vo =e rsa
V(r) = 0 Lea (30)
are hu

We do not tabulate U)(a) and k} for this potential,
as the recurrence relations (equation 19) show
that with the form (equation 30), the values are
exact in the zeroth order for the reduced width
and exact to first order in the energy eigenvalue,
dene

(i) U,(a) = W, (a)

i
A
iN)
+
<

(ii) ke

" ae and (32)

“(ae
Au Au AU

!
w
iT]
(or)

(iii) Be = 0 forn> 0.
Preston's values, slightly modified for g,
are:

g = -0.3826 , a = 9.62

which gave q = -2.37 x 10-3, the exact result.

It is important to note how different the
higher order values are for U,(a) and kj for each
potential. This illustrates that the effective
range approximation does not contain enough
information to determine higher energy parameters.

COMPUTATION OF INTERACTION MATRICES BY QUADRATURES

Perturbation theory allows the calculation of
bound state wave function and energy eigenvalues,
as well as the scattering phase shifts for most
commonly used potentials. As part of this theory,
it is necessary to evaluate integrals of the form:

a
en ve)? (a) nN, | an VO 54% _

fe)
a
16x a
where
cee : Oe fa
GH, Az) = J,4@) 5
(32)
2 1
eae re ate a
r a :
Oa
and J, ,1(z) is the ordinary Bessel function. The

XQ are*the infinite set of solutions to the
eigenvalue equation

(X = 0 (33)

Jy 1%o)
and 'a' is the usual matching radius of the reac-
tion matrix theory. V(r) is a local potential
with restrictions on its behaviour near r = 0, or
"a'. We call quantity (32) the ‘interaction
matrix'.

For some commonly used potentials, such as
the Woods-Saxon, analytic results are not avail-
able for Vo; so numerical methods must be used.
We have discovered that ordinary schemes, such

as the trapezoidal rule, Simpson's rule and Gaussian
quadrature, give satisfactory results in test cases
for small A and u. However, for A,pu > 10, the
Bessel functions in integral (32) oscillate with
increasing speed and conventional schemes fail to
give accurate answers unless a superfine integra-
tion increment is used. As this is costly in com-
puter time, we have developed a quadrature scheme
which makes use of the particular form of (32).

The interaction matrix (32) is basically
different to that defined by Cook (1972) in that if
U,{r) is the reaction matrix wave function evaluated
in the presence of the interaction V(r), Cook's
matrix is

a
ve = | dr V(x)U, (r)W (x) 5 HW) = N (2)
(34)

which is related to equations (32) by the trans-
formation

V=eBW (35)

where B is the overlap integral

a
oa = I dr U, (r)W (1) (36)

The physical significance of equation (35) is that
V° is the 'bare' interaction matrix which, analo-
gous to quantum field theory, is the transition
energy between vacuum states |A» and |y>. The
transformation (4) 'clothes' the bare interaction
matrix and gives the transition energies between
vacuum states |y> and interacting states |\>.

THE QUADRATURE SCHEME

It is assumed that the potential is given at a
set of M points such that

4 AV)
Cay Vii) Nie ; regs Se.
where (37)
Tn tm-1
(ii) ve =V | |

Dropping the & superfix, the integral (32) becomes
fo) a Un
Crees Sl ) v2 |

Un-1

du J, (XW, Oy) (38)
To proceed further we need to evaluate the integrals
in (38) analytically.

Consider the integral (Abramowitz and Stegun
(1964):

Z
2.42
[ (XF-X7)t JO t)T, (Xt)
= 2{X) J, (X25 (X 2) -X F(X 2), OK 293
(39)

Changing the notation to the functions j, (2) and
using (8), we find that

58 J. L. COOK AND OTHERS

ee ree)

m m+1
(40)
{XJ g.y XI, Ou -X, 5, uF, Ou}

for }\ # u

and, employing 1'Hopital's rule, the diagnonals
become

2
Ls mn mem on

(41)
f Fyn Udy 4d}

COMPUTATIONAL RESULTS

The above quadrature scheme was checked
against the exact formulae for the Yukawa,
Gaussian and exponential potentials. A 500 point
scheme gave excellent agreement (to within 0.5%
for A,u < 20) for values of a < 500. The error
in this scheme increases with increasing 'a', but
decreased with increasing number of points. For
errors less than 2%, 500 points gave satisfactory
results up to a = 1000, 1000 points up to a = 2000
and 2000 points up to a = 4000. Extending the
X,;u range up to 40 increased the discrepancies to
about 1.5% for a < 500.

It seems that doubling the number of points
in the quadrature scheme extends the a-range by a
factor of two, however, this is at the expense of
computing time which is also doubled. We feel
confident that the quadrature scheme with 500
points is good enough to predict v¥ to within
0.5% of the exact value for any potential V(r) and
a ¢ 500. Potentials with a singularity at the
origin can also be handled by setting u, very
small, but not zero, which leads to negligible
error.

INTERACTION MATRICES

(a) Linear Potential

Let V(r) = gr, where g is a coupling constant.

Then for s-waves

yo? = tga Z

AU ra 2
(X, 2X)
where the plus sign is taken for (i,u) even-even

or odd-odd, and the minus sign for (\,y) even-odd
and odd-even. For \ = u, one gets

for } # u (42)

oO _ 1 1
V4 = ga E > (43)
in which X, = K,a. These formulae were checked
with the quadrature scheme which gave a difference
of less than 0.2% for a 1000 point and 0.5% for a
500 point quadrature.
(b) Harmonic Oscillator

For this case

V(r) = gr? (44)

and
oO _ 2 ‘ 32 =f)
pe = tga [OX x) +(%4%,) ] for \ # u (45)
yoo = ga’ 1 + =e e (46)
AA 3 2
2X)

This was also checked with the quadrature scheme
(<0.5% for 500 point quadrature).

(c) General Power Law Potential

This example has

V(r) = gr" (47)
for which
Lo 1 n
Ce = V(a) I, du u jg (XW, vw)
= V(a) oe (48)

in which gu

Nt is independent of ‘a’.

Although a general form for this quantity is
not reported elsewhere, it can be seen that the
perturbation series generates an expression in
which each term is a power of V(a) and is an
ordinary power series.

(d) Inverse Power Law for Large Radius

V(r) = gr Pt 0 <6 <1 (49)
We use the approximation
comeei ;
Le v | dr V(L)N, Jp (K, TIN, 5 (Kr) 3 (50)

the resulting integral is given by Erdélyi et al.
(1953) as

(1) he = K 2Fi(atsb'3c"3z) (51)

in which a' is not the cutoff radius, but

(ii) at = Q41-- 5 ;
(iii) b'=5 (1-0),

(Gav)5y “C\sse hit 2 ;

2 2
si si
(v) z =— =-— _ and is independent of ‘a'

LS Xt where i < u

2F, is the usual hypergeometric function,

: ee ils Q+5 1
(vi) C= 2 NAN, KK Ky T(a')
ih
(vii) M=2° (kane Pr(e')r(ct-a'-b')

For the s-wave case, and 'a' large, the numer-
ical results from these equations for p = 1 agree

COMPUTATION OF REACTION MATRIX PARAMETERS ay

with Coulomb scattering results, the Yukawa case
with zero shielding coefficient and the quadrature
scheme.

(e) Generalised Yukawa for Large Radius

Let V(r) = ee ee ; a > 0 (53)
Erdélyi et al. reported the result
; Lo C
Gs) Vou anes M ’
in which K. > Ky
ie TT
Gale C= > NNKK |,
Ge Mae 2a) Be nce)
~S P(a+2v+2m) -Ku yn
(iv) jie . aes | Sx
nog m!T(v+m+1) 482
7 (54)
Kebab eu; Z)
(v) a' = -m 5)
(vi) b' = -(v+m) ;
Gay. et = velar 4 > :
Ke, ecko
(viii) z+—-+=— and is independent of a;

The series (54) is numerically useful for only
very large 'a' and converges specifically for
|K /28| <1, ise. a> (%,/268)a1 Thus 1t does not
converge for high order A or u.
(f) Generalised Gaussian for Large Radius
We write
2
V(r) = pie ae , (55)

and use the Erdélyi et al. result
' Lo _ _C
Gi) Vo= ey 4 ; (56)

(ii) C=2NN VKK ;

-y $tv
Gia) owe Za KD g2 T(c!)
¢ co r{ > >'] ake m
eee . oy m!T(c'+m) | 48 :
x oF2(a'5b'5€'5a) ;
Where =o 2s RN eX
K2 x? r u
u u
(vi) a' = -m ;
(vii) b' =-(vtm) ,
(viii) cl =vel=2+ ;

Again, this series fails if \ or u are large. It
was checked satisfactorily with the quadrature

scheme and the exact formula (26) for a = 2.
(g) Ordinary Gaussian for Large Radii

For this case

2
Viaje ee (57)
and Erdélyi et al found that
oa
; Sas —
kO_ oT yor 4B a
Li a) en Se 28 eS ae | 28 (58)

This case provides a good test example for general
quadrature schemes. I (2) is the associated
Bessel function.

THE WOODS-SAXON POTENTIAL

The contribution of Coulomb fields to the
region external to the matching radius 'a' of
reaction matrix theory was first derived by Wigner
and Eisenbud (1947). Normally, one takes 'a' to
be equal to the finite range of the strong nuclear
interaction. The collision matrix S, for each
partial wave is then given for elastic scattering
and one channel open by

1-R.L 2i6
; 7 a2) _ Q
(i) Sy = 2, | ar e (59)
LoL
where Ry is the reaction matrix,
(11) Ly = S,+ip,-B, .
Gia) s. = ta | fertkr)sF2 (kr)
De eee eC yee Q r=a ’
and
. 2 2 2
(iv) Ee = ka[G) (ka) +F) (ka) ] ;

k is the centre of mass momentum and Fy, and Gy are
the Coulomb regular and irregular wave functions
respectively. We have

216)
(Vv) 8, =e - BH =e

=tan7? holes
oo G (ka)

is the Coulomb hard sphere phase shift. Such a
formalism can be extended to include any long-
range force and poses no problem in nuclear reac-
tion theory.

A typical optical potential was used by Moake
and Debevec (1980) to fit data from elastic
proton scattering on ®Li, 17C and 1*N at 144 MeV
proton energy. If we try to derive a reaction
matrix from their potentials, particular interest
in the convergence of the series is paid to

(a) internal Coulomb fields,
(b) the Woods-Saxon potential, and

(c) the L*S coupling contribution.

60 J. L. COOK AND OTHERS

First we discuss (a) and (b) in general and avoid
the complication of having to deal with a two-
component wave function.

No analytic results have been found for the
bare interaction matrix ah in the case of the
Woods-Saxon potential. This has the local form

-V
V(r) = — (60)
x
1l+e
where x = (r-rA)/Y
r_= a basic nuclear radius parameter,

A = the atomic mass of the target
nucleus,

y = the diffusivity of the nuclear
surface,

V_ = the depth of the potential well
within the nuclear volume

and we define

Ri = TOA (61)

as the nuclear radius.

The form (60) was substituted into the quad-
rature formula given in section 4 and the bare
interaction matrix evaluated for the s-wave case.
The Moake and Debevec parameters in the Heaviside
units are, for Tt NGS

(1) = 0.03337
(11) Y = 5.5618 (62)
(111) Ro = 28.865

The resulting matrix was substituted into our
perturbation series with a = 50 and the higher
order terms of the wave function and energy
eigenvalues in the case of the first ten reson-
ances. Beyond order N = 2, the series began to
diverge rapidly and no realistic combination of
‘a’ and N gave convergence. This result is sur-
prising, and the Woods-Saxon form is very like a
square well for which our series gives exact
results to zero order in the reduced widths and
to first order in the R-matrix poles. Tracing
through the terms in our series, we found that
the interaction between surface and volume con-
tributions appeared to produce the divergence.

We then tried separating the surface contri-
bution from the volume contribution by defining
the surface potential as

V(r) = -V | : | +V_, r<R
(e) ox oO fe)
1lt+e
(63)
-V
= ~ 5 r>R
l+e 2

This form converged after twelve iterations. From
the knowledge that addition of a square well con-
tribution to any potential does not change the
eigenfunctions U,(a) and shifts the energy eigen-
values k, by Vo, we can subtract Vy from the final

converged values of k¥ to obtain the correct eigen-
values for the Woods-Saxon case. Using the Moake-
Debevec parameters (62), we obtain the resonance
parameters shown in Table 4 for the first six terms.

TABLE 4
RESONANCE PARAMETERS FOR A WOODS-SAXON POTENTIAL

2
r U, ky
0 0.2139 -0.0350
1 -0.1618 ~— -0.0219
2 0.2291 -0.00975
3 -0.1782 0.0158
4 0.2104 0.0473
%) -0.1947 0.0856

With this simplified version of the Moake-Debevec
potential we did not try to patch the bound levels
with those of '®0 as the internal Coulomb field,
the L*S contribution and the imaginary part of the
optical potential were not included. The chief aim
was to test the convergence of our series for a
reasonable nuclear potential.

Such potentials as the Moake-Debevec usually
alter the Coulomb potential to a charge-distribu-
tion potential at radii corresponding to the edge
of the nuclear charge distribution. However, the
value of 'a' corresponding to the limit of the
strong interaction is often considerably larger
than this; consequently, there is interest in the
perturbation produced by the Coulomb component of
the interior potential. This can be computed in
two ways.

(a) The original technique of Born (Schiff
1949) wherein a screened potential is used

276 :
V(r) = exp{-6r} , e = electric charge
7 (64)
to produce an interaction matrix for s-wave and
large 'a' of

2 252 ong

vee % re and 2 B°+(Atutl) ot : (65)
u a2B2+(A-u) 202

The factor 2 comes from the coefficient 2M, where

M = reduced mass. Substituting this matrix into

our series and allowing the screening coefficient
8 to tend to zero produces the limit

Atutl
gn ; (66)
| A-u|

oo 2Ze?
>

Au a

resulting in a logarithmic divergence for the self-
interaction terms of Vo. This is raised to the nth
power in the expression for the nth order perturba-
tion to the wave-function and energy eigenvalue.
Renormalisation of the coupling constant could be
introduced, as in quantum electrodynamics, for the
diagonal terms alone, but this procedure gives an
incorrect answer.

(b) The exact expression for the Coulomb
interaction matrix for s-waves and any value of
Val sis

COMPUTATION OF REACTION MATRIX PARAMETERS 61

oo 2Ze
oe = [C, ((24+1) 1) -y-2n((2y+1) n)]
m2zes
er 2
oo Whe |
Vj€2) #u) = S— 4C, (C-u) 1} -C, (Ctu+1) 1)
Atut1
gn - (68)
|>-n|
Da2Ze-
pa OG .
where y = Euler's constant and
wane hy dt
C,(z) = - j cos t es (69)

as defined by Abramowitz and Stegun (1964). The
logarithmic singularity apparent in (66) is
explicitly subtracted in (68). If a Coulomb radius
Y, 1S introduced to define the edge of the charge
distribution, the interior Coulomb interaction is
just

oO

= 2
Vy, = 22e7G, (70)
in which
Gos : SU oa ix)
AU u Joo u
fe)
X= (A+3) 0 ; (71)

and j,(2) =f J1 (2)
= sin z

A useful method for spot checking the s-wave
interaction matrix elements is as follows. An
approximation to the integral is taken from the
general form of the s-wave interaction matrix:

a

cos Kr dr ; (72)

use r-r

O

This may be written as

fo) fe)
sin Kr Y
re) e
fe)
Y
© l+t+e
a
cos Kr
+ = ote or
re)
Oo 1 +-e if

Substituting v = r-rpo in the first integral
and u = r=? in the second integral, we get

Sin Kr o cos K (r_-v)du
- fe)
I(K) = 4 - / +
deepest
fe)
a-T5 cos K (r,+u)
+ aa aan TT cae du
beer |
fe)
in K i
iv Peat gas at : sin Ku du
Vie ee Sin K tT, PET OS
6 ie

The integral is a tabulated standard form given in
Gradshteyn and Ryzhik (1965) and leads to the final
result:

Ty Sin K Ts

US SS ia a

tae : (73)

The s-wave interaction matrix becomes

00 2g T T
a 1((a-u) J )-T(Qatu+1) 2 )| . (74)
CONCLUSION

The mathematical framework for computing the
reaction matrix from a given potential has been
presented from the point of view of perturbation
theory. Although entirely numerical methods could
be used to compute the relevant parameters, this is
very time-consuming, even on modern computers. In
such a technique, the wave equation has to be
integrated many times to search for the eigenvalues,
then integrated to r = a to find the U,(a), followed
by similar procedures for each partial wave. Our
method of mostly analytical solutions is much
faster.

The concept of the interaction matrices, both
bare and clothed, is much clearer in the forward
problem than in the inverse one. From this theory
one finds the following:

(i) The interaction matrices and the overlap
matrix are completely determined by the
local or non-local potential. There is
no manifestation of phase equivalence.

(ii) The bare interaction matrix is always
symmetric. In general, the overlap
matrix is not.

Ongoing investigations based on this work have
allowed us to find a simple way of representing
local potentials from the above matrices.

REFERENCES

Abramowitz, M. and Stegun, J., 1964. Handbook of
Mathematical Functions. Dover Publications
Inc., New York.

Chadan, K. and Sabatier, P.C., 1977. Inverse
Problems in Quantum Scattering Theory.
Springer-Verlag, New York.

62 J. L. COOK AND OTHERS

Clayton, E., 1972. The inverse scattering problem:

a numerical calculation of T-N interactions.
M.Sc. thesis, University of New South Wales.

Cook, J.L., 1972. Aust. J. Phys. 25, 167.

Erdélyi, A., Magnus, W., Oberhettinger, F. and
Tricomi, F.G., 1953. Higher Transcendental
Functions, Vol. II. McGraw-Hill, New York.

Gradshteyn, I.S. and Ryzhik, I.M., 1965. Tables
of Integrals, Series and Products. Academic

Press, New York, p. 480.

Hartt, K., 1980. Phys. Rev. C 22, 1377.

Lane, A.M. and Thomas, A.G., 1958. Rev. Mod. Phys.

J.L. Cook, E.K. Rose, and B.E. Clancy,
Lucas Heights Research Laboratories,
Private Mail Bag,

Sutherland, NSW, 2232, Australia.

30, 257.

Moake, G.L. and Debevec, G.L., 1980. Phys. Rev.
Ci2dy 25%,

Newton, R.G., 1966. Scattering Theory of Waves
and Particles. McGraw-Hill, New York, p. 280.

Preston, M.A., 1965. Physics of the Nucleus.
Addison-Wesley, Reading, Mass., p. 27.

Schiff, L.I., 1949. Quantum Mechanics. McGraw-
Hill, New York, p. 149.

Wigner, E.P. and Eisenbud, L., 1947. Phys. Rev.
72, 29.

(Manuscript received 30.10:1983)
(Manuscript received in final form 26.1.1984)

Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 63-66, 1984

ISSN 0035-9173/84/010063 — 04 $4.00/ 1

Notes on Freshwater Zooplankton Found in Central Province,
Papua New Guinea, 1981-2

BAREND VLAARDINGERBROEK

ABSTRACT.
Papua New Guinea between 1981 and 1982.

The study reported on was carried out on three water bodies in Central Province of
They were Lake Surinumu, a hydroelectric reservoir on

the Sogeri Plateau, which was ascertained to be warm polymictic and oligotrophic, Waigani Swamp

in Port Moresby, and the artificial pond at Varirata National Park.
are discussed in terms of their local ecology and zoogeography:

The following zooplankton
the Rotifers Brachtonus falcatus,

Asplachna brightwelli, Trochosphaera aequitortalts, and Filinta opoltensts; the Crustaceans
Diaphanosoma sarst, Dtaphanosoma exctsum, Certodaphnta cornuta, Eodiaptomus lumholtat,
Thermocyclops crassus, Mesocyclops leuckarti and the genus Phyllognathopus; and the Dipteran

planktonic larva Chaoborus.

INTRODUCTION

Prior to 1980 very few species lists for the
Papua New Guinea limnetic fauna had been put
together. Between 1980 and 1982 I collected
zooplankton samples from three water bodies in
Central Province and also some physicochemical data.
With the exception of one rotifer all species were
identified by Professor C.H. Fernando of Waterloo
University, Canada, and Dr. N.N. Smirnov of the
Academy of Sciences, USSR.

The water bodies sampled were:

(i) Lake Surinumu, a hydroelectric reservoir on
the Sogeri Plateau, an impoundment of the Laloki
River at an altitude of 538 m.a.s.1. The lake is
shallow (I recorded a maximum depth of 14 m) with
a complex perimeter. Petr (1976) reported a fall
in nutrient ion concentration between 1970 and 1975
and commented on the lake's very low calcium

concentration, in the range of 0.075 - 0.090 meequils

having been raised to its present level in 1971.

(11) Waigani Swamp, a shallow tropical body at
sea level in Port Moresby, which has been a site of
sewage effluent disposal since 1975.

(111i) The artificial pond at Varirata National
Park, altitude approx. 750 m.a.s.1. It was no
deeper than 2.25m at any time when I sampled it.

METHODS

A standard silk-bolt net was used for all
zooplankton sampling. Lake Surinumu was sampled
regularly between October 1981 and December 1982 at
various points throughout the lake. Littoral
samples were taken at Waigani Swamp on three
occasions in 1982 in response to a request from
Dr. R. Hamond of Melbourne University while a
surface tow was taken in December 1982. The pond
at Varirata was visited twice in 1982.

Physicochemical parameters were measured at
Lake Surinumu only. Water levels and surface
temperatures were recorded throughout 1982 while
surface water samples were submitted to the

University of Papua New Guinea in June 1982 for
nutrient and photosynthetic pigment analyses.

RESULTS

(1) Lake Surinumu - Physicochemical: The lake's
water level was observed to peak at 13.5m as
measured at the dam wall in March following the

wet season influx, while the lowest watercolumn at
the same site was 6.5m in December. At the same
time surface temperatures generally rose from 27 C
to 31.5 C. Nutrient concentrations in March were
found to be consistently low throughout the lake,
featuring Soluble Reactive Phosphorus concentrations
of 3 ug.L’! while NHy,-Nitrogen readings ranged from
120 - 215 ug.L ! Nutrient levels in the May and
June surface water samples were much lower

(maximum NO3-Nitrogen recorded was 25 ug.L 1)
although there was an increase in S.R.P. concentrat-
ions to a maximum of 8 yg.L !.

(ii) Lake Surinumu - Productivity: Only the March
samples were analysed. The maximum chlorophyll-a
pigment concentration measured was 7.14 ug.L
while the maximum carotenoid concentration was 7.00
m.S.p.u.

(i111) Lake Surinumu - Colonial Cyanophytes: Two
genera were regularly found in samples, namely
Microcystts and Osctllatoria. Microcystts was
found to be most abundant from July to December
1982 while Osctllatorta was very abundant from
March to July 1982.

(iv) Zooplankton Found: (at Lake Surinumu only
unless specified)

Rotifers:

Brachtonus faleatus, perenially present in low
abundances.

Asplachna britghtwellt, perenially present in low
abundances, peaking in November 1981, with a
relatively high abundance recorded in March
1982 in a shallow basin in which many
ephippial and juvenile cladocerans were also
present.

64 BAREND VLAARDINGERBROEK

Trochosphaera aequitorialts, found at all times
except June to September 1982, very abundant
October to December 1982 (maximum relative
abundance 0.64 in November, 1982.

Filinta opoltensts, present in very low abundances
between June and December 1982. Owing to the
species' similarity in appearance to B.
falcatus and to the fact that sample analysis
could not begin until October 1982, by which
time earlier samples had been stored in
formalin for several months, it is quite
possible that specimens in those samples were
not recognized.

Crustaceans:

Dtaphanosoma sarst and Diaphanosoma exctsum, at
Lake Surinumu and Waigani Swamp. The two
species can be distinguished from one another
only by the shape of the fold on the exo-
skeletal margin and this was not possible for
most samples due to preservation damage. The
diaphanosomids in the December 1982 Waigani
Swamp sample were however described as
D. exetsum by Professor Fernando in the
apparent absence of its congener, while my own
observations of identifiable specimens indicat-
ed that D. sarst is the more abundant in Lake
Surinumu. The density of diaphanosomids at
Lake Surinumu peaked at 2.6 organisms per
litre in January 1982 with secondary peaks in
May and July 1982 approaching 2.5L !, with
troughs of about 1 organism per litre from
February to May 1982 and fewer than 0.1 L !
from September to December 1982. Fertility in
terms of percentage ephippial females featured
a single peak in March 1982 of nearly 40%.

Certodaphnia cornuta, at all three sites. At Lake
Surinumu the species was perennially present,
featuring relative abundance peaks of 0.55 -
0.6 from December 1981 to March 1982 with a
secondary peak of 0.48 in October 1982, the
lowest abundance recorded being 0.1 in July
1982. Ephippial females were perennially
present peaking at 38% in March 1982.

Eodtaptomus lumholtzt, at Lake Surinumu and
Varirata. At Lake Surinumu this species is
normally dominant, a peak relative abundance
of 0.82 being recorded in August 1982, though
the animal fell to below 0.1 in October 1981
and November to December 1982.

Thermocyclops crassus, at Lake Surinumu and Waigani
Swamp, perennially present in the former, and
very abundant in the December 1982 Waigani
Swamp sample.

Mesocyclops leuckartit, perennially present in low
abundances.

Phyllognathopus, a single specimen of which was
found in littoral samples at Waigani Swamp.

Insect Larva:

Chaoborus, present in low abundances in all samples
except those taken from June to October 1982.

DISCUSSION

Lake Surinumu would appear to be of the warm
polymictic type by Hutchinson and Loffler's thermal
classification of lakes (1956). Neither thermal
stratification nor tropholytic oxygen depletion
tend to occur in such lakes (Bayly and Williams,
1973; Finlayson, Farrell and Griffiths, 1980). Both
Petr's (1976) and my own nutrient analyses indicate
that the Lake is oligotrophic by Finlayson and
Gillies (1982) trophic classification for artificial
lakes.

B. falecatus is characteristic of tropical lakes
in general, and occurs in subtropical and temperate
regions (Ruttner-Kolisko, 1974). Specific
references to it include the Lower Murray River
(Shiel, Walker and Williams, 1982), the Queensland
University Pond (Timms, 1967), the Lake Kainji
Reservoir and the potamoplankton of the Niger and
Swashi Rivers (Clarke, 1978a), and the Eilengele
Reservoir in Nigeria (Imevbore, 1967), where it is
reported to display an optimal temperature range of
1294

A. brightwelli features a very wide tropical
and subtropical distribution, both limnetic and lotic
(Fernando et al, 1982). References to it include
the Lower Murray River (Shiel, Walker and Williams,
1982), the Queensland University Pond (Timms, 1967c),
Eilengele Reservoir (Imevbore, 1967), and the Blue
Nile River (el-Moghraby, 1977). A predaceous
carnivore, its diet includes B. falcatus and
juvenile cladocerans (Green and Oey, 1974),
consistent with my observations of its high
abundance in the basin featuring a high abundance of
ephippial cladocerans in March 1982.

The global distribution of 7. aequttortalts
has been poorly mapped (Fernando, 1980). It occurs
commonly in the Danube Delta (Ruttner-Kolisko, 1974)
and is common in Sri Lankan lakes (Fernando, 1980).

F. opoltensts is a pantropical species (Ruttner-
Kolisko, 1974). It is common in India (Koste and
Shiel, 1980) and in the Blue Nile (el-Moghraby, 1977.

The distributions of the diaphanosomids are
complicated by the fact that a degree of uncertain-
ty exists about 'species' identifications in many
reports prior to 1980. Krovchinsky (1981) noted
that specimens from New Guinea and Celebes classif-
ied as D. pauctsptnosum by Brehms in 1939 were
almost certainly D. exctsum while reports of D.
sarst from Sars in 1901 were probably D. spinulosum,
and suggested that all reports from Africa were
particularly suspect. Fernando et al (1982)
reported that D. exctsum is an exclusively tropical
species. The species appears to be common in
Queensland and New South Wales (Krovchinsky, 1981)
and it was reported as being present in Lakes
Dakataua and Wisdom in Papua New Guinea's West New
Britain Province (Ball and Glucksman, 1982).
Krovchinsky (1981) reported D. sarst as definitely
occurring in North Queesland and Sumatra. Both
species occur in Sri Lanka, D. exctsum being more
common in reservoirs while D. sarst is more common
in rivers and ponds (Rajapatska and Fernando, 1982).
The genus appears to display a marked preference for
calm waters in the temperature range of 27 - 28.5 C
in Lake Surinumu, especially in terms of its
univoltine reproductive cycle.

FRESHWATER ZOOPLANKTON 65

Ceriodaphnia cornuta is a pantropical species
which extends into subtropical regions (Fernando et
al, 1982), being common in tropical Asia, Africa,
America and Australia (Rajapatska and Fernando,
1982). It featrues a high abundance in the White
Nile Gebel Aulia Dam (Clarke, 1978), Lake Kainji
and the Blue Nile (el-Moghraby, 1977). It is a
common limnetic species in Australia and normally
peaks in spring or summer, though in Tasmania it
does so in winter (Bayly and Williams, 1973), and
was reported from Lake Dakataua by Ball and
Glucksman (1982). It was recorded as being
multivoltine in Lake Surinumu, but fertility peaks
appeared to correlate inversely with density,
suggesting that lowering population densities acted
as a parthenogenetic stimulus.

Eodiaptomus lumholtat is one of two species
of a genus present in Australia, inhabiting the
open waters of lakes, large ponds and deep pools
(Willisms, 1968). Bayley (1966) reported its
distribution as being from the north-east of West
Australia, across mid-Northern Territory to a
southerly latitude of 23S. This distribution
appears to be due to mutually exclusive competitive
relationship with Boeckella trtarttculata (Bayly,
1965). Bayly (1965) claimed a similar relationship
exists between F. lunholtzt and Calamoecta species,
but Bayly and Williams (1973) stated that where the
two coexist, competition for food is avoided by the
two species growing to different average sizes.
With the exception of samples in which both £.
lumholtat and C. cornuta were at a low abundance,
the Correlation Coefficient between the relative
abundances of the two species as measured at the
dam wall in Lake Surinumu was found to be -0.88,
indicating intense interspecific competition,
C. cornuta being relatively the more abundant until
June 1982, with £. lumholtzt more so from June on.
It is possible that temperature is responsible for
this change in competitive status, higher
temperatures favouring the latter.

T. crassus is a globally widespread species
(Fernando et al, 1982).

M. leuckartt is a cosmopolitan species
exhibiting considerable ecological diversity though
it is seldom dominant (Gophen, 1978b). It is
omnivorous but will not eat Microcystis (Clarke,
1978b). It preys on both Ceriodaphnta and
Diaphanosoma species. It is common in the Blue
Nile (el-Moghraby, 1977), Lake George in Uganda
(Burgis, 1974), Lake Kainji and the Swashi and
Niger Rivers (Clarke, 1978a), Lake Kinneret in
Israel (Gophen, 1978a), and Lake Tjeukemeer in the
Netherlands (Vijverberg, 1977), as well as in New
South Wales lakes and reservoirs (Bayly and
Williams, 1973) and in Victorian waste stabilizat-
ion ponds (Mitchell and Williams, 1982).

Phyllognathopus occurs in Europe, North
America, Northern Africa, the Malay Archipelago,
Brazil, Patagonia and New Zealand (Barclay, 1969).

Chaoborus is a pantropical dipteran genus
extending into subtropical regions (Fernando et
al, 1982) which preys on diaphanosomids,
copepodites, and adult cladocerans, cyclopoids and
calanoids (Lewis, 1977, 1979).

ACKNOWLEDGEMENTS

I wish to extend my gratitude to Professor
C.H. Fernando, Waterloo University, Canada; Dr. N.N.
Smirnov, Insitute of Evolutionary Morphology and
Ecology of Animals, Academy of Sciences, U.S.S.R.;
and the staff of the University of Papua New Guinea,
Biology Department.

REFERENCES

Ball, E. and Glucksman, J., 1980. A Limnological
Survey of Lake Dakataua, a Large Caldera Lake
on West New Britain, Papua New Guinea, with
Comparisons to Lake Wisdom, a Younger Nearby
Caldera Lake. Freshwat. Btol., 10, 73-84.

Barclay, M.H., 1969. First Recrods of a New
Species of Phyllognathopus (Copepoda:
Harpacticoids) in New Zealand. WN.Z. J. Mar.
& Freshwat. Res., 3, 296-303.

Bayly, I.A.E., 1965. The Australian Species of
Diaptomus (Copepoda: Calanoida). Aust. J. Mar.
& Freshwat. Res., 17, 123-134.

Bayly, I.A.E., 1966. The Australian Species of
Dtaptomus and Their Distribution. Aust. Jd.
Mar. & Freshwat. Res., 17(1), 123-134.

Bayly, I.A.E., and Williams, W.D., 1973.
Waters and Their Ecology. Hawthorn:
Aust. Pty.

Inland
Longmans

Burgis, M.J., 1974. Revised Estimates for Biomass
and Production of Zooplankton in Lake George,
Uganda. Freshwat. Btol., 4, 535-541.

Clarke, N.V., 1978a. A Comparison of the
Zooplankton of Lake Kainji and of the Rivers
Swashi and Niger. Hydrobtologta, 58(1), 17-23.

el-Moghraby, A.I., 1977. A Study on the Diapause
of Zooplankton in a Tropical River - the Blue
Nile (Sudan). Freshwat. Btol., 7, 207-212.

Fernando, C.H., 1980. The Freshwater Zooplankton
of Sri Lanka, with Discussion of Tropical
Freshwater Zooplankton Composition. Int. Rev.
ges. Hydrobtol., 65(1), 85-125.

Fernando, C.H., Sephton, D.H., Rajapakse, R., Jeye
T., and Matsumura-Tendisi, T., 1982. An
Illustrated Guide to Tropical Freshwater
Zooplankton. In print when a copy sent to me
by Fernando.

Finlayson, C.M., Farrell, T.P., and Griffiths, D.J.,
1980. Studies of the Hydrobiology of a
Tropical Lake in North West Queensland. Aust.
J. Mar. & Freshwat. Res., 31, 589-596.

Finlayson, C.M., and Gillies, J.C., 1982. Biologi-
cal and Physicochemical Characteristics of the
Ross River Dam, Townsville. Aust. J. Mar. &
Freshwat. Res., 33, 811-827.

Cophen, M., 1978. The Productivity of Mesocyclops
leuckartt (Claus) in Lake Kinneret (Israel).
Hydrobtologica, 60(1), 17-22.

66 BAREND VLAARDINGERBROEK

Green, J., and Oey, B.L., 1974. Asplachna and the
Spines of Brachtonus calyetflorus in Two
Javanese Sewage Ponds. Freshwat. Btol., 4,
223-226.

Hutchinson, G.E., and Loffler, H., 1956. The
Thermal Classification of Lakes. Proc. Nat.
Acad. (Set. sU.5. A. 5 42, "84-36.

Imevbore, A.M.A., 1967. Hydrology and Plankton
of the Eilengele Reservoir, Nigeria.
Hydrobtologta, 30, 154-176.

Koste, W. and Shiel, R.J., 1980. Preliminary
Remarks on the Characteristics of the
Rotiferan Fauna of Australia. Hydrobtologia,
TS Lot 227 «

Krovchinksy, N.M., 1981. Taxonomic and Faunistic

Revision of Australian Dtaphanosoma (Cladocera:

Sididae). Aust. J. Mar. & Freshwat. Res., 32,

813-131.

Lewis, W.M., 1977.
Tropical Chaoborus population.
btol., 75 311-325.

Feeding Selectivity of a
Freshwat.

Lewis, W.M., 1979. Zooplankton Community
Analysis - Studies on a Tropical System.
Springer-Verlag, New York. Inc.

Mitchell, B.D. and Williams, W.D., 1982. Factors

Influencing the Seasonal Abundance and

Occurrence of Zooplankton in Waste Stabilizat-

ion Ponds. Aust. J. Mar. & Freshwat. Res.,

33, 989-997.

Barend Vlaardingerbroek,
P:O. Box 1135,
Ayr, Qld., 4807, Australia.

Petr, Ts, 1976. Some Chemical Features of Two
Papuan Fresh Water Lakes (Papua New Guinea).
Aust. J. Mar. & Freshwat. Res., 27, 467-474.

Rajapatska, R., and Fernando, C.H., 1980. The
Cladocerans of Sri Lanka (Ceylon) with Remarks
on Some Species. Hydrobtologta, 94, 49-70.

Planktonic Rotifers -
Dte Binnengewasser,

Ruttner-Kolisko, A., 1974.
Biology and Taxonomy.
26(1) Suppl.

Shiel, R.J., Walker, K.F., and Williams, W.D., 1982.
Plankton of the Lower River Murray, South
Australia. Aust. J. Mar. & Freshwater Res.,
$3, 301-327.

Timms, B.V., 1967. Ecological Studies on the
Entomostraca of a Queensland Pond with Specific
Reference to Boeckella minuta Sars (Copepoda:
Calanoida). Proc. R. Soc. Qld., 79(5), 41-70.

Vijverberg, J., 1977. Population Structures, Life
Histories and Abundances of Copepods in
Tjeukemeer, The Netherlands. Freshwat. Btol.,
7, 579-597.

Williams, W.D., 1968. Australian Freshwater Life-
the Invertebrates of Australian Inland Waters.
Sun Books, Melbourne.

(Manuscript received 14.5.1984)

Journal and Proceedings, Royal Society of New South Wales, Vol. 117, pp. 67-70, 1984

ISSN 0035-9173/84/010067 — 04-$4.00/ 1

Changing Employment Patterns and Truncated Development
in Australia*

Hon. BARRY O. JONES. M.P., MINISTER FOR SCIENCE AND TECHNOLOGY

I welcome this opportunity to speak to the
Royal Society of New South Wales. It seems
particularly appropriate to be with you at a time
when the Australian Reserve Bank has chosen to
commemorate John Tebbutt (1834-1916), a distinguish-
ed Fellow of your Society, on the $100 note, a
hopeful augury, as I told the Treasurer, of future
support for astronomical ventures.

It is commonplace to say that we live in an
era of unprecedented technological, social and
cultural change. JI am inclined to think that ours
is one of the two most rapid periods of change, the
other being the three decades of the 'belle epoque'
before World War I. The French philosopher Charles
Péguy argued that 'in the period 1880 to 1913 the
world has changed more than in the time since Jesus
Christ.

This period was marked by the development of
telephones, electrified cities, motor cars, gramo-
phones, radio, cheap photography, motion pictures,
mass circulation newspapers, X-rays, aircraft and
aerial bombardment, not to mention post impression-
ism, Cubism, jazz, Stravinsky's Rifes of Spring,
quantum theory, relativity (E = mc) and Sigmund
Freud.

I want to begin by talking about the changing
patterns of work in Australia and then go on to
discuss the Canadian concept of ‘truncated
development' which seems to be, I regret to say,
an appropriate description of our situation.

Australia in my view has gone through a 'post
industrial revolution' since the 1960s, with a
paradigm shift in employment and trade away from the
development model of the post-World War II era. In
my book Sleepers, Wake, my essay ‘Industry and
Development' and in my Labor Economists Lecture
"Technology, Development and Employment', I have
discussed these shifts at length.

In Sleepers, I set out in an Appendix what I
impertinently called 'Jones' Seven Laws'. If I
rewrote the book now, I would add an eighth, although
in importance I would place it first.

"Employment levels are culturally determined'.

It is the culture which determines whether a 16
year old should be at school or in the labour force
or whether the appropriate retirement age is 55, 60,
65 or 70. This is not to discount economic factors
(which come first in most analyses) and human
psychology as well.

However, I would argue that it is postcodes
which determine life-styles and life-changes far
more than technology. A recent survey by the N.S.W.
Education Department indicated a more than 90%
retention rate for high school pupils in the Bligh
state electorate, including Woollahra (2025)
compared to less than 15% in the electorate which
includes Broken Hill (2880) - that is, of Year 1
school entrants, there was a more than 6:1 differ-
ence in the numbers who stayed on to Year 12.

* Address delivered before the Royal Society of
N.S.W. on the occasion of the Annual Dinner on
21st March, 1984 at the University of Sydney.

Regional, class and ethnic factors are all
critical in determining employment aspirations and
employment levels.

In "working class' areas it is taken as
absolutely axiomatic that the great majority of
fifteen to nineteen year olds will be in the labour
force competing for work. In "middle class"
electorates there are totally different aspirations.

In addition, as Raymond Williams the doyan of
English social critics has pointed out we have
adopted the very odd principle (that has been built
into modern English education) that those who are
slowest to learn should have the shortest time to
learn, while those who learn quickly will be able
to extend the process of learning for as much as a
further seven years.

For two hundred years ever since the Industrial
Revolution began, we have taught people that life
without work is meaningless and when work is
withdrawn, not surprisingly, people feel diminished

"Middle class" people with their adaptability
and flexibility, enter the labour force late, often
in their 20s, move in and out of careers and
localities as easily as they move in and out of
marriages, they break continuity with working
holidays and overseas travel, and can leave work
early or late as it suits them without worrying too
much about whether they will have 35, 40, 45 or 50
years of it. They are generally relaxed about
adapting to new technology. People employed in the
new 'Information' sector are overwhelmingly
"middle class". '"Working class" people suffer from
considerable cultural rigidity, often being anchored
to a particular job type and to a specific region.
Home ownership is a factor which ties them to
declining regions - 'Who would buy my house if I
move?', they ask. They often start work at 15,
expecting a 50 year end-on stretch (long service
leave notwithstanding). They dare not get off the
treadmill, even temporarily, for fear of not gett-
ing back on. At 65, many self destruct when
compulsory exclusion from work means the curtail-
ment of income, some loss of life's purpose and an
end to the primary social relationship, often
followed by rapid physical deterioration.

Australia's capacity to adopt and pay for an
appropriate range of life and work styles for its
people will depend to a large extent on whether we
are able to take advantage of development
opportunities selectively and quickly.

"TRUNCATED DEVELOPMENT' AND THE 'X' INDUSTRY

On a recent visit to Canada (January 1984) I
was struck by the almost morbid resemblance between
many elements of the Canadian and Australian
economies: both of us immensely resource-rich, but
with the commanding heights of the economy in
foreign hands, manufacturing in long-term decline,
a reduced share of world markets and a sense of
frustration about failure to match rates of growth
in newly developing nations.

I was grateful to be able to discuss these
problems in Ottawa with officers of the Science
Council of Canada, the equivalent of ASTEC, and in
Montreal with members of the GAMMA Institute, a

68 HON. BARRY O. JONES, M.P.

think-tank comprising staff from the Montreal,
McGill and Concordia Universities and the Ryerson
Polytechnic. (GAMMA had some parallels with
Melbourne University's Institute of Applied Econom-
ic and Social Research until its recent changes).

Dr. J.M. Gilmour, Director of Research at the
Science Council, delivered a valuable paper 'The
Industrial Policy Debate in a Resource Hinterland'
at a symposium held by the Academy of Technological
Sciences in Canberra in October, 1981 on
"Manufacturing Resources of Australia' (Gilmour,
1982), and I draw heavily on it for what follows
in the next section.

The Canadians apply the useful term 'truncated
development' to describe a superficial, stunted
form of industrialisation, characteristic - at
least until very recently - of their economy and
still true of ours. As Gilmour says, after World
War II, 'tariffs promoted industrialisation by
invitation', but this promoted products rather than
indigenous firms and to a large extent foreign
factors of production - capital, technology and
management - substituted for local ones.

‘Truncation occurs when a subsidiary does not
carry out all the functions - from original
research to marketing - necessary for developing,
producing and selling its goods' and also describes
the general tendencies of foreign firms to allocate
roles to subsidiaries which serve the global
interest of the parent, such as limitation to an
assigned market.

There are several adverse consequences of
truncation:

T. Subsidiaries are unable to initiate new
products or develop new markets and are
increasingly dependent on the parent. Factors
which would encourage innovation, flexibility
and producing new products for world markets
are almost invariably absent.

Zs The diminished structure of subsidiaries makes
them dependent on the parent for components,
subassemblies, designs, services and finished
goods for resale with adverse effects on the
balance of payments, significantly reducing
the multiplier effect of industrial growth.

3. Foreign owned subsidiaries are constrained
from exporting, first because they never
intended to do so, and second because they are
usually assigned products that have no
international sales potential. (In Canada
when foreign firms export these are predomin-
antly intra-corporate transfers and not part
of free-market trading).

4. The range of employment generated in local
subsidiaries is limited to management,
process work, transport and routine services:
there is little if any scope for professional,
scientific, assigned and overseas marketing
functions.

Sn Th¢re is a severely dampening effect on
technological capacity and innovation. 'Most
subsidiaries are technologically dependent,
have little or no innovation capability, and

are unable to generate products with internat-
ional sales appeal.' When multinationals
transfer technology it is done in such a way
that it rarely results in a spin-off of
technological capability to other local firms.
There is no problem with technology transfer -
the products of Ford, Hoechst, Union Carbide or
ICI are only a telex or telephone call away - ©
but only the branch office benefits directly.

Canada had the reputation of being the only non-
banana republic with a higher degree of foreign
economic penetration than Australia.

Certainly the percentage of effective foreign
ownership in major industries in Australia was
extraordinarily high in the last year they were
recorded (1972-73) and there is little to suggest
that the pattern has changed since then:

Motor Vehicles 99.8%
Plastics 94.3%
Processing aluminium 91.2%
Petroleum 90.8%
Agricultural chemicals 85.7%
Basic chemicals 78.0%
Pharmaceuticals 77.8%
Industrial chemicals 75.2%
Electronics 69.3%

9%

Construction equipment 59.

In Canada, as in Australia, classical econom-
ists and free-marketeers have blamed the failure of
manufacturing on short production runs and sub-
optimal production scales and, as Gilmour says,
"took a theological leap in directly and wholly
attributing ... competitive problems tc tariff
protection'. This was naive and superficial without
considering the basic problem of trunction. To
condem as non-competitive industries in Australia
which were explicitly programmed not to compete
seems to be as unfair and absurb as insisting that
non-vertebrates should show some backbone.

Australia has been consistently decreasing its
dependence on tariffs but has been unfairly condem-
ed as hard line because it has been frank about
honestly declaring its tariff position. Other
countries are notorious for applying non-tariff
barriers. Even within the ostensibly free-trade
European Common Market, the transfer of certain
goods from, say, Germany to France can be madden-
ingly slow, uncertain and frustrating - far more
costly than the imposition of a tariff. The
problems of placing many of our products in Japan
where severe import quotas are imposed are legendary.

In Canada, as in Australia, an alternative
economic view to the free-marketeers is being put
both inside and outside the Government and public
service, that of the economic 'nationalists' who
argued that interventionist policies were needed
(before all tariff protection disappeared) to
prepare for international competition. This meant
combatting the combined impact of high costs, low
productivity, general technological weakness, lack
of innovation and lack of entrepreneurial
initiative.

Gilmour identifies five major areas of concern
by Canada's economic nationalists (and you will
judge for yourselves their relevance here):

CHANGING EMPLOYMENT PATTERNS 69

in "Excessive reliance on the development of
natural resources is undesirable. The nature
of international trade is changing and the
areas of Canada's traditional strength are now
facing increasingly sharp competition.

De "Resources are not sufficient to offset
deficits in secondary manufactures and
services', and he points to Canada's total
dependence on imported capital equipment in
drilling, excavating, mining, oil and gas.

3 "The high capital intensive nature of resource
extraction presents few opportunities for large
scale employment growth' and Canada's unemploy-
ment rate was consistently the highest in the
OECD during the 1970s and is higher than
Australia's now.

4. "Any shift in demand away from Canada's export
staples or any bottleneck in supply . would
pose a crucial threat to the Canadian economy'.

5: ‘The complement to a large trade surplus in
staples is a large deficit in finished
manufactured goods. This is the staple trap
Canada's trade surpluses are generally found
in those commodities for which the long-run
income elasticity of demand is quite low. This
means that as foreign incomes grow, demand for
those products grows less than in proportion
to income. In contrast, Canada's deficits are
in manufactures and service, i.e. items for
which the income elasticity of demand is
fairly high'.

The Canadians have put a heavy emphasis in the
last two years in focussing their efforts ina
comparatively few areas, applying the 'niche'
approach with success. Being part of that enormous
North American economic engine can be both a threat
and an opportunity. The danger of overlay by their
powerful southern neighbour is always present (the
analogy of making love to an elephant has often
been used) and for a long time Canadians seemed to
have a permanent and massive inferiority complex
("Being Canadian means always having to say you're
sorry'). On the other hand the sheer size of the
North American market - when opportunities open up -
and physical ease of penetration make it potentially
very lucrative. The Canadians have gained world
markets with telecommunications equipment,
specialised computer applications, the impressive
'Telidon' on-line data bank, instrumentation and
process controls and some space technology.

Bell Canada, Mitel, Northern Telecom, Infomat,
Glenayre, Western Research, Bytec-Conterm and many
others have internationally recognised brand names-
in Australia we have none. It is not that we have
a bad reputation in brand name goods - we simply
have no reputation at all.

We used to export Australia's Sunshine
Harvester - now the brand name belongs to Canada's
Massey- Ferguson.

For Australia and Canada there is a need to
recognise the changing international environment,
and there are penalties for slow learners.

World markets are approaching saturation for

a widening range of products of which cars and TV
sets are obvious examples and this has been
accompanied by the rapid growth in productive
capacity from newly industrialised countries - South
Korea, Taiwan, Hong Kong, Mexico and Brazil. The
large scale aircraft industry appears saturated

with only two firms - Boeing and Airbus - still in
contention.

There is another factor which deserves notice.
I drew attention to it in Sleepers, Wake! and so
does Gilmour 'The occurrence of major product
innovations with the power to create large and
entirely new markets and industrial branches has
been slowing down over the last forty years (in
part due to the cyclical nature of
innovation) The tremendous expansionary benefits
from the last great burst of major product
innovations have been harvested'. As I wrote
in Sleepers, where is the 'X' industry which some
unthinking technological optimists assert will
arise in manufacturing in the same way that cars,
planes and electrical industries arose in the past?
The inventive peak of what I have called the 'Third!'
Industrial Revolution' occurred between 1942 and
1970, coinciding with the era of full employment.
The 1970s marked a significant decline in major
discoveries, although many new technological
refinements were produced. In aviation, for
example, the jumbo jet dates from 1968 and the
supersonic Concorde from 1969: the wide-bodied jets
of the 1970s were not innovative. In micro-
electronics, large-scale integrated circuits dated
from 1969 and the micro-processor from 1971.
Magnetic bubble memories were developed in 1966
and the 'Josephson junction' in 1968: since 1970
their capacity has increased enormously, but again
few new concepts have emerged. Orbiting space
laboratories and communications satellites were
put into service in the 1970s based on techniques
first used during the space race nearly twenty
years earlier. Lasers and radio telescopes were
products of the 1960s.

Clearly service employment will continue to be
the overwhelmingly dominant employer for the
foreseeable future.

In 1780 John Adams, later to become the second
President of the United States wrote these words
from Paris to his wife Abigail:

‘I must study politics and war that my sons
may have liberty to study mathematics and
philosophy. My sons ought to study
mathematics and philosophy, geography, natural
history, naval architecture, navigation,
commerce and agriculture in order to give
their children a right to study painting,
pocery , Music. architecture, Statuary,
tapestry and porcelain.'

This reflects the concept of the 'hierarchy of
needs' which the psychologist Abraham Maslow wrote
about in his Mottvation and Personality and which
is abundantly illustrated in the changing nature of
our labour force. Humanity starts with basic needs
for food, water, shelter and goods on to increasing
needs for gourmet cooking, Perrier water,
sophisticated and specialised habitations, both
stationary and mobile, together with individual
demands for information, leisure and culture. We

70 HON. BARRY O. JONES, M.P.

move away from staples towards CD players and
Mozart piano concertos.

The option is still open to make the 1980s a
creative era in which as Dennis Gabor has said,
Mozartian man (or woman) can evolve.

REFERENCES

Gilmour, J.M., 1982. The Industrial Policy Debate
in a Resource Hinterland, 7m Manufacturing
Resources of Australia, Symposium, Academy
of Technological Sciences in Canberra,
October, 1981.

Jones, B.O., 1982. Sleepers, Wake! Technology
and the Future of Work. Melbourne: Oxford
Univ. Press. 285p.

Jones, B.O., 1983. Technology, Development and
Employment. Labor Economists Lecture,
Sydney.

Jones, B.0O., 1983. Industry and Development, in
Drummond, LABOR ESSAYS.

Hon. Barry O. Jones, M.P.

Minister for Science and Technology,
Parliament House,

Canberra, ACT, 2600, Australia.

(Manuscript received 21.3.1984)
(Manuscript received in final form 6.6.1984)

REPORT OF THE COUNCIL FOR THE YEAR ENDED 3Ist MARCH, 1984 71

MEETINGS

Nine general monthly meetings and the annual
meeting were held during the year. The average
attendance was 23 members and guests (range 11 to
42). Summaries of the addresses were published in
the Newsletter and abstracts of the proceedings are
appended to this report.

The Clarke Memorial Lecture for 1983 was
delivered by Associate Professor R.H. Vernon on
"Restite, Xenoliths and Microgranitoid Enclaves in
Granites" at Macquarie University on 21st September
1983. The text is published in the Journal and
Proceedings, Volume 116, pages 77-103.

Council held 11 ordinary meetings during the
year. From April to November 1983, the meetings
were held in the Board Room, Science Centre,
Sydney; in February and March 1984, they were held
at Macquarie University. In addition there were
held: one extraordinary meeting of the Council on
15th June, 1983, two extraordinary meetings jointly
with the Council of the Linnean Society of New
South Wales on 13th April and 27th May, 1983, six
meetings of a joint committee of representatives of
the two societies on 15th and 30th June, 14th and
28th July and 11th and 25th August, 1983, and one
special meeting of the Royal Society Executive on
23rd August. These additional meetings were
necessitated by the failure of Science House Pty.
Ltd. and the consequent impending loss by both
societies of their library and office accommodation
upon sale of the Science Centre.

At its meeting on 1st February, 1984, Council
established a Working Party to examine the Society's
operations and recommend future directions which
the Society could realistically pursue. One meet-
ing of the Working Party, on 24th February, had
been held by the close of the Society's year.

ANNUAL DINNER

The Annual Dinner was held in the Withdrawing
Room, Sydney University Union, on the evening of
Wednesday, 21st March, 1984. 59 members and guests
were present. The Guest of Honour was Mr. Barry
Jones, B.A., LL.B., M.P., Minister for Science and
Technology in the Australian Government. Mr. Jones
gave an address entitled ''Changing Patterns of
Employment and Truncated Development'"'. The vote
of thanks was moved by Professor T.W. Cole, Vice-
President.

PUBLICATIONS

Journal and Proceedings Volume 116, Parts 1
to 4 were published during the year, incorporating
14 papers and the 1982-83 Annual Report. Council
is again grateful to the voluntary referees who
assessed papers offered for publication.

Every effort is made to ensure the wide
availability of the Journal in Australia and
overseas. In addition to the copies automatically
sent to members 444 copies were distributed as
follows: 241 to exchange partners, 115 to

subscribers and 88 as donations (mainly to
university libraries which do not have suitable
exchange publications to offer). Counting these
three categories together, 98 copies go to the
United States, 52 to Great Britain and Ireland, 23
to Japan, 20 to Canada, 18 to U.S.S.R., 12 to New
Zealand, 11 to West Germany and 7 to South Africa;
copies also go to 43 other countries.

The Journal is abstracted routinely in Chemical
Abstracts, Physical Abstracts, Geological Abstracts,
Geoabstracts, Mathematical Reviews, and when
relevant, in Biological Abstracts.

Newsletter

Nine issues were published. Council is most
grateful to the authors of short articles, which
are much appreciated by members.

MEMBERSHIP

The membership of the Society at 31st March,
1984 was:-

Honorary Members 12
Company Member 1
Life Members 33
Ordinary Members 288
Absentee Members 12
Associates Zh

Total 367

AWARDS
The following awards for 1983 were made:
Walter Burfitt Prize:

Edgeworth David Medal:
Archibald D. Olle Prize:

Dr. William Stephen Hancock
Dr. Denis Wakefield

Mr. David S. King and

Dr. Nicholas R. Lomb

Citations follow this report
SUMMER SCHOOL

A most successful Summer School on "Sound" was
held from 16th to 20th January, 1984, at the CSIRO
National Measurement Laboratories, Lindfield. 42
students who had completed high school year 11
attended the School. The program comprised lectures
and tutorials on a wide variety of topics, including
the physics and mathematics of sound, sonar and
sound propagation in the ocean, ultrasonics and its
use in measurement and medical diagnosis, noise and
noise pollution, earthquake waves, hearing,
electronic music and the making of musical instru-
ments. Visits were paid to the Ultrasonics
Institute of the Department of Health at Millers
Point and the Mastertouch Piano Roll Company at
Petersham.

LIBRARY

With the sale of the Science Centre building
appearing imminent all reader services and inter-
library loans were ceased at 5.00 p.m. on 28th
April, 1983. The possible fate of the library was

ANNUAL REPORT OF COUNCIL

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ANNUAL REPORT OF COUNCIL 18

investigated by Council, and it soon became
apparent that the Society could not afford to
retain the major serials collection as a working
library. It was resolved therefore that, if
possible, a suitable recipient be sought who would
be willing to take over the serials collection as
a working unit, make it available for reference
within a reasonable time, and make some permanent
public acknowledgement of the donation.

In the event offers to take over the collect-
ion were received from the N.S.W. Institute of
Technology and the University of New England.

After lengthy deliberation Council resolved that
the collection of serials be donated to the Dixson
Library of the University of New England. This
decision was confirmed by members at the Ordinary
General Meeting of 6th July, 1983. The Society has
retained its collection of historic monographs,
early scientific journals and some other Australian
publications.

Transfer of the collection to Armidale took
place in July/August at the University's expense,
and involved packing and moving over 1000 boxes.
The Dixson Library has reestablished the major
unique part of the collection as a separate unit
under the title of ''The Royal Society of New South
Wales Collection" which will be displayed promin-
ately on a brass plate. The Library is producing
a catalogue of the 1,100 titles involved in the
donation, and every volume will bear the Society's
crest stamped in gold and include a bookplate
acknowledging its source.

Involvement in the inter-library loans system
has recommenced already and the former Journal
exchange arrangements will continue.

Council expresses its sincere gratitude to
the Honorary Assistant Librarian, Mrs. Grace
Proctor, particularly for her valuable assistance
with the transfer to the Dixson Library.

OFFICE

A joint committee consisting of the Executives
of the Royal and Linnean Societies was established
in May with a view to finding suitable joint office
assommodation. This committee met several times
between June to August, and bodies such as the
National Trust, the State Government and various
tertiary institutions were approached as well as
commercial real estate companies. An offer of the
use of space in the Fisher Bookstack was made to
this Society by the University of Sydney. After
the sale of the building in October the Linnean
Society decided to reestablish its office at North
Sydney.

The Council of Macquarie University resolved
in November to make available to the Royal Society
part of Convocation House at 134 Herring Road,
North Ryde, which is on the University campus and
was being used as a temporary book depositary.

This offer was accepted by the Society's Council
and it is anticipated that the house will become
available and the Society's office be re-establish-
ed there by the end of May 1984. In the interim
period temporary office accommodation has been
generously provided for the Society by its Honorary
Treasurer and Assistant Secretary, Drs. A. and J.

Day, at their home in Lindfield. Council is
exceedingly grateful to the Day household for this.

The office at Macquarie University will house
the Society's collection of journals and monographs,
which have been in commercial storage, and should
provide a meeting and reading room for members.
Part-time membership of the Macquarie University
Club also will be available to Society members.

SCIENCE HOUSE PTY. LTD.

Since the inception of the project the Society's
four directors on the Board of Science House Pty.
Ltd. have been: Mr. M.J. Puttock (Vice Chairman,
and since mid-1979, Chairman), Mr. E.K. Chaffer,

Mr. J.W. Humphries, and Associate Professor W.E.
Smith. Following his appointment as editor of the
Australian Mathematical Society's Journal Professor
Smith found it impossible to continue as director
and resigned with effect on 31st March, 1983. Dr.
A.A. Day was appointed in his place by Council on
27th April. Board meetings were held on 6th, 23rd,
24th and 30th (two) May, and 6th and 15th June.

The Board's principal concern was with the serious
financial situation of the Company, income being
inadequate to cover normal outgoings and the large
interest bill on the loans from the Commonwealth
Bank. In September 1982, with the Bank's encourage-
ment 3 floors of the Science Centre building had
been offered for sale under strata office title, but
no sale had eventuated. In March 1983 the whole
building was put up for sale by private treaty and
on 24th May, 1983, it was offered for auction

but without attracting any bids. Concurrently the
Board was actively examining possible ways of
retaining the secretariat (servicing scientific and
other bodies) with or without the meeting room
facilities. A detailed report on the room hire
operation was obtained from a leading firm of
chartered accountants.

Following the unsuccessful attempted sale of
the building by auction the Board sought and receiv-
ed detailed advice from the Company's solicitors
and auditor. Representatives from the Board met
senior management of the Bank on 26th May and 3rd
June. On 6th June the Board resolved to proceed to
wind up the Company as soon as possible. On 15th
June the Society's Council and the Board passed the
formal resolutions necessary to achieve a Creditors'
Voluntary Winding-Up in the manner specified by the
Companies (New South Wales) Code, 1981. Meetings
of shareholders and creditors were convened on Ist
July. The meeting of shareholders (represented by
their Presidents, Dr. R.S. Vagg and Dr. C.N.
Smithers) passed the following special resolution:

"That it has been proved to the satisfaction

of this meeting of members of Science House

Pty. Limited that the Company cannot, by reason

of its liabilities, continue its business, and

it is advisable to wind-up, and accordingly
that the company be wound-up voluntarily and
that Richard John Grellman of 167 Macquarie

Street Sydney be nominated as Liquidator for

the purpose of winding up."

Mr. E.K. Chaffer attended the meeting of creditors
as the appointed director required by the

Companies Code, and was elected chairman of that
meeting. The Society, as creditor, was represented
by Dr. A.A. Day. In addition to the Linnean
Society, the Bank, the restaurateur, the Company's

74 ANNUAL REPORT OF COUNCIL

employees and the Liquidator were also present.
The Society's Proof of Debt (Form 131) was handed
in setting out its claim for approximately

$420,000. A "Report as to Affairs" (Form 30) was
distributed showing (in summary):
Assets: $4.3 M
Amounts owing: 5.7 M
Net assets: 0.6 M
Claims by employees 0.1 M
Estimated Amount available for
unsecured creditors: 0.48M
Unsecured creditors § contingent
liabilities: 0.84M
Estimated deficiency, subject to
costs of liquidation: $366,861

A Committee of Inspection representing the
creditors, was appointed, consisting of Mrs. R.J.
Inall (employees), Dr. A. Ritchie (Linnean Society)
and Dr.A.A. Day (Royal Society) to meet with the
Liquidator as required. As from the closure of the
meeting the Board of the Company ceased to exist,
its powers being taken over by the Liquidator.

The Science Centre secretariat was deemed by
the Liquidator not to possess any inherent monetary
value and in August was transferred to the Science
Centre Foundation Ltd. at no charge. A slight
improvement in the previously depressed office
real estate market having emerged, the Liquidator
put the Science Centre building up for sale by
auction on 12th October, 1983, and it was sold
after brief bidding for $3.775M.

At 31st March, 1984 the liquidation of Science
House Pty. Ltd. had not been completed.

F INANCE

The Annual Accounts, prepared as usual by
Messrs. Wylie and Puttock, Chartered Accountants,
show firstly a loss on the year's operations of
$2505, and secondly, a writing off of the assets
of the Resumption Reserve of $416,991. The
principal factors producing the deficit were the
rejection by the N.S.W. Government of our applic-
ation for a grant (possibly connected with the
same policy of reducing support for scientific
research indicated by the closure of research at
Sydney Observatory), an increase in printing costs
due to a welcome increase in the size of the
Journal and Proceedings, an unwelcome substantial
increase in postal costs of the Journal, and costs
associated with the enforced removal of the
Society's library, office and Journal back-issues
from Science Centre. A substantial increase in
investment interest and increased membership
subscriptions were insufficient to balance those
increases in costs.

The probable writing off of the loan to
Science House Pty. Ltd. was foreshadowed in last
year's report and was inevitable following the
failure of the sale of the Science Centre building
to realise sufficient return to cover all outstand-
ing debts to the Bank and other secured creditors.
The Society ranked as an unsecured creditor for its
loan, as did the Linnean Society.

We are again grateful to Mr. A.M. Puttock of
Messrs. Wylie and Puttock for his helpful advice

in the resolution of the many financial problems
which have arisen during the year.

NEW ENGLAND BRANCH REPORT

Officers: Chairman: S.C. Haydon
Secretary: R.L. Stanton

Committee: T. O'Shea

H.G. Royle

Branch Representative
on Council: S.C. Haydon

The following meetings were held:

1983

6th June Professor E.B. Burnside,
University of Guelph, Canada on
"The role of genetics in food
production - mice, men, computers
and cows".

26th June Professor Ian Falconer, Dr.

Maria Runnegar and Dr. Arthur
Beresford, University of New
England, on ''Blue-green algal
toxins from Malpas Dam. Their
nature, effects and how to remove
them from drinking water".
23rd August Professor E.F.W. Seymor,
University of Warwick on "Modern
magnetic methods emerge from the
laboratory - astronomy, archaeol-
ogy, anatomy".
14th September Professor Theresa Brophy,
University of Queensland, on
"Not only the Broad Street pump".
19th October Dr. Terry Speed, Chief of the
Division of Mathematics and
Statistics, CSIRO, on ''The
assessment of risk; a statistic-
ian's view".
14th November Professor T.W. Cole, University
of Sydney, President of the
Royal Society, on "Our future in
communications and computing".
1984
29th February Professor C.N. Watson-Munro,
University of Sydney, on "Does
the world need nuclear power".
27th March Professor A.E. Ringwood,
Australian National University,
on "Disposal of high-level
nuclear wastes - a geological
perspective".
9th April Mr. J.O. Reynolds, Manager
Corporate Affairs, Western
Mining Corporation, on ''The
Roxby Downs operation: mining
methods and precautions".

ANNUAL REPORT OF COUNCIL We

FINANCIAL STATEMENT OF THE NEW ENGLAND BRANCH

Balance carried forward, 1.4.83 $177.40
Subvention from Royal Society, Sydney 150.00
Bank Interest 8.83
$336.23
Less Expenses: -

Meeting 11.10.82 $40.00

1429.55 74.00

Us 14.11.83 36.15

Us 29, 2.84 154.55

um 27 Soa 51.95

Federal Govt. Tax 0.40
$356.65
Balance carried forward, 31.53.84 $ (20.42)

ACKNOWLEDGEMENTS

In conclusion, the Council wishes to express
its gratitude to the many people who assisted the
Society in the past year, including:- Associate
Professor J.H. Loxton, Mrs. M. Krysko and Professor
T.W. Cole who organised the Summer School; Professor
S.C. Haydon and Professor R.L. Stanton in the New
England Branch; Mr. K. Schmude and Mr. W. Callaghan
for organising the transfer of the Royal Society
Collection to the Dixson Library; and Mrs. Grace
Proctor and Mrs. Judith Day for their assistance in
the library and office.

Plates 2 and 3. Views of the "Royal
Society Collection" on temporary
shelving at the Dixson Library,
University of New England, Armidale.

Photos: kK. Schmude

FINANCIAL STATEMENTS FOR THE YEAR ENDED 3lst DECEMBER,

76

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80 ANNUAL REPORT OF COUNCIL

ABSTRACT OF PROCEEDINGS 1983 - 1984

The Annual General Meeting and nine General
Monthly Meetings were held in the Science Centre,
35 Clarence Street, Sydney. Abstracts of the
proceedings of these meetings are given below. In
addition the Clarke Memorial Lecture was delivered
on 21st September, 1983 by Associate Professor R.H.
Vernon at Macquarie University. The title of the
Lecture was ''The Trouble with Granites".

APRIL 6th

947th General Monthly Meeting. Location: the
Auditorium, 1st Floor, Science Centre. The
President, Professor T.W. Cole was in the Chair
and 42 members and visitors were present. John
Huon Brown was elected to membership. Paper read
by title only: "Precise Observations of Minor
Planets at Sydney Observatory during 1982" by N.R.
Lomb.

116th Annual General Meeting. Followed the
947th General Monthly Meeting. The Annual Report
of the Council and the Annual Statement of Accounts
were adopted.

The Clarke Memorial Medal was awarded to
Emeritus Professor Noel Charles William Beadle;
the Edgeworth David Medal to Dr. Nhan Phan-Thien;
and the Royal Society Medal to William Broderick
Smith-White.

Messrs. Wylie and Puttock, Chartered Account-
ants, were elected Auditors for 1983.

The following Office-Bearers were elected for
1983/84:

President: Dr. R.S. Vagg

Vice-Presidents: Professor T.W. Cole,
Dr. G.S. Gibbons, Mr. M.J. Puttock,

Professor B.A. Warren.

Mr. E.K. Chaffer

Mrs. M. Krysko

Dr. A.A. Day

Hon. Secretaries:

Hon. Treasurer:
Hon. Librarian: Mr. J.L. Griffith
Members of Council: Dr. R.S. Bhathal,
Mr..D.S. King, Assoc. Professor J.H.
Loxton, Assoc. Professor D.H. Napper,
Mr. M.A. Stubbs-Race, Dr. F.L. Sutherland
Dr. W.J. Vagg, Professor S.C. Haydon
(New England Representative)

The Presidential Address "The Technological
Revolution in Communication and Computing" was
delivered by Professor T.W. Cole.

The incoming President, Dr. R.S. Vagg was.
installed and introduced to members.

MAY 4th

948th General Monthly Meeting. Location: the
Auditorium, 1st Floor, Science Centre. The
President, Dr. R.S. Vagg, was in the Chair and 22
members and visitors were present. Professor
John Manning Ward was elected to membership.

An address entitled ''The Museum of Applied
Arts and Sciences" was delivered by the Director,
Dr. L.G. - Sharp.

JUNE Ist

949th General Monthly Meeting. Location:
Room G, lst Floor, Science Centre. The President,
Dr. R.S. Vagg, was in the Chair, and 27 members and
visitors were present. Richard Hoskin Read, Roy
Malcolm MacLeod, and Dennis John Frost were elected
to membership.

Papers read by title only: "The volatile leaf
oils of Melaleuca armillarts, M. dtssitiflora and
M. trtchostachya"' by J.M. Brophy and E.V. Lassak;
"Silcretes in the Cobar Area, NSW" by R.A. Glen and
J.T. Hutton; "Basement/cover relations and a Silur-
ian I-type intrusive from the Cobar-Lucknow area,
NSW'' by R.A. Glan, G.L. Lewington and S.E. Shaw;
and "Lake Dieri and its Pleistocene environment of
sedimentation" by J.A. Dulhunty.

An address entitled ''Natural Food Flavours"
was delivered by Dr. F. Whitfield, of the CSIRO,
Division of Food Research, North Ryde.

JULY 6th

950th General Monthly Meeting. Location:
Room E, 2nd Floor, Science Centre. The President,
Dr. R.S. Vagg, was in the Chair and 22 members and
visitors were present. Richard Arthur Glen, Kylie
Maitland Mattocks and Richard Hewitt Christopher
Carrington were elected to membership. Paper read
by title only: '"'Astrometric Determination of Mass
Segregation and Membership Probabilities in Galactic
Clusters" by D.S. King.

Following a resolution of Council made on 15th
June, 1983, the.Meeting decided that the Royal
Society Collection of scientific serials be donated
to the Dixson Library, University of England.

An address entitled "Lasers and their
applications" was delivered by Dr. K. Crane of the
CSIRO, Division of Applied Physics, Lindfield.

AUGUST 3rd

951st General Monthly Meeting. Location:
Room J, 2nd Floor, Science Centre. The President,
Dr. R.S. Vagg was in the Chair and 11 members and
visitors were present.

An address entitled "Cacti in Australia" was
given by Mr. W. Harland of "Booalbyn" Orchard,
Wedderburn.

SEPTEMBER 7th

952nd General Monthly Meeting. Location:
Room J, 2nd Floor, Science Centre. The President,
Dr. R.S. Vagg was in the Chair and 20 members and
visitors were present.

An address entitled "Offshore Petroleum
Exploration - Sydney Basin" was delivered by Dr.
T.G. Russell of the Sydney 0il Company Limited.

OCTOBER Sth

953rd General Monthly Meeting. Location:
Room H, 2nd Floor, Science Centre. The President,
Dr. R.S. Vagg was in the Chair and 20 members and
visitors were present. Peter John Derrick and
Joseph John Brophy were elected to membership.

ANNUAL REPORT OF COUNCIL 81

NOVEMBER 2nd

954th General Monthly Meeting. Location:
Room H, 2nd Floor, Science Centre. The President,
Dr. R.S. Vagg was in the Chair and 18 members and
visitors were present.

Vincent Chi-Kin Lau and David St. Clair Black
were elected to membership.

Papers read by title only: ''Stratigraphy
and Sedimentation of the Late Permian Illawarra
Coal Measures in the Western Coalfield, Sydney
Basin, NSW'' by C.S. Bembrick; ''The Technological
Revolution in Communication and Computing"
Presidential Address by T.W. Cole; ''Lambdarina
(Rhynchonellacea) from the Upper Visean of Queens-
land" by R. Nazer; "The Teaching Hospital: Past
Present and Future" by J.B. Hickie; ''Sydney
Southern Star Catalogue" by D.S. King and N.R.
Lomb; and ''Dextral Movement on the Demon Fault,
Northeastern New South Wales: a Reassessment" by
J. McPhie and C.L. Fergusson.

An address entitled ''Trace Elements and Coal
Combustion'' was given by Dr. D.J. Swaine, Leader,

Geoscience Section, CSIRO, Division of Fossil Fuels,

North Ryde.

DECEMBER 7th

955th General Monthly Meeting. Location:
Room H, 2nd Floor, Science Centre. The President,
Dr. R.S. Vagg was in the Chair and 25 members and
visitors were present.

It was announced that the office on the 6th
Floor of the Science Centre had closed at the end
of November, and a new office would open at
Macquarie University early in 1984.

An address entitled 'Minerals, Gems and
Volcanoes" was delivered by Dr. F.L. Sutherland,
Curator of Rocks and Minerals, Australian Museum,
Sydney.

CITATIONS

THE JAMES COOK MEDAL

"In Australia, only three species of arachnids are a serious threat to the life and health of man.
These are the red-back spider, the Sydney funnel-web spider and the common bush tick''. S. Sutherland,

1976.

Dr. Struan Keith Sutherland has devoted his considerable talents to the investigation of the venoms
and toxins present in the Australian environment particularly those provided by spiders. The aim of these
investigations is to provide the people of this country with effective treatment should they be bitten by

venomous spiders.

From a firm base of the analysis of the effects of spider bite he proceeded in his research with
characterizing specific venoms both biochemically and biologically.

Venoms are a peculiarly potent group of agents from a biologist's viewpoint and often provide

startling and sometimes lethal effects.

Investigations of the activity of venoms have been fruitful in

determining the various components of the coagulation cascade and they can act as a tool to nibble away at
obdurate problems involving understanding of biochemical functions.

Dr. Sutherland is the Foundation Head of the Immunology Research Department of the Commonwealth Serum
Laboratories, Melbourne and has contibuted substantially to our understanding of the mode of action of
venoms peculiar to Australia and to the rational formulation of the most effective measures of treatment

of the affected persons.

Dr. Sutherland was born in 1936 and educated at Bendigo High School and Melbourne University.

He served in the Australian Navy as a Surgeon Lieutenant from 1962 to 1965 on the HMAS Voyager and
Melbourne. Appointment to the staff of the Royal Melbourne Hospital followed and he has held an appoint-

ment as Clinical Assistant since 1966.

He won the AMA Prize for Medical Research in 1977 and has been a visiting lecturer at the
Universities of Sydney and Melbourne and at Monash University.

He has written extensively in his area of expertise and his more significant publications include
Dangerous Animals and Plants of Australia (1979), Venomous Creatures of Australia (1981) and Australtan

Animal Toxins (1983).

82 ANNUAL REPORT OF COUNCIL

As previously deserted areas of Australia are settled there is the likelihood that diseases and
toxins as yet not clearly defined will come to the fore and be recognised. It is essential that we have
active Departments such as those headed by Dr. Sutherland to cope with identification and formulation of
treatment of previously obscure envenomation.

The James Cook Medal of the Society originates from gifts by Mr. Henry Ferdinand Halloran over the
period 1943-44, It is awarded for outstanding contributions to Science and Human Welfare in and for the
Southern Herispehre. Dr. Sutherland is a worthy recipient of the James Cook Medal for his work on the
venoms peculiar to Australia.

THE WALTER BURFITT PRIZE AND MEDAL

The Walter Burfitt Prize and Medal was founded by Dr. and Mrs. W.F. Burfitt for scientific work done
in Australia or New Zealand and was first awarded in 1929.

The recipient of the 1983 award is Dr. William Stephen Hancock. Dr. Hancock is a Reader in the
Department of Chemistry, Biochemistry and Biophysics at Massey University, Palmerston North, New Zealand.
He heads an active research group concerned with lipoprotein chemistry and the chemical synthesis of
peptides and proteins. Over the six year period 1977 to 1982 his research group has published fifty
papers associated with these topics and is highly regarded by both the reviewers for the National Heart
Foundation of New Zealand and the Medial Research Council of New Zealand.

He has put forward a new concept in the study of the structure-function relationships of proteins
which he has called "active site engineering" and his group is the holder of a patent involving an
"activated matrix" system. The metabolism of lipoproteins is of great importance in the understanding of
coronary atherosclerosis and Dr. Hancock has performed basic work in this field.

THE EDGEWORTH DAVID MEDAL

Dr. Denis Wakefield graduated M.B., B.S. with Ist Class Honours in the University of New South Wales
in 1976. Graduation prizes included the Australian College of Ophthalmologists Prize, the Graduation Prize
for Surgery and the University Medal for Medicine. He is a member of the Australian Society of Immunology,
the Australian Society for Medical Research and is a Fellow of both the Royal Australasian College of
Physicians and the Royal Australasian College of Pathology.

During the last four years Dr. Wakefield's research has mainly involved the immunology of the eye and
in particular the relationship between certain genetic factors and the role of bacterial infections in
causing ocular inflammation. He was the first person to outline the aetiology of uveitis in an Australian
population and first to describe the relationship between the blood group HLA B27 and the most common form
of uveitis. His was the first description of the HLA antigens and other immunogenetic markers of uveitis
and retinal vasculitis in an Australian population. As a result of Dr. Wakefield's work it is now realised
that some 50% of patients with anterior uveitis have the HLA B27 blood group antigen.

Dr. Wakefield has made some outstanding scientific discoveries in relation to the immunological
mechanisms responsible for controlling the body's immune response to the Chlamydia trachomatis micro-
organism which is responsible for the epidemic of trachoma in the Aboriginal population of this country.
His results have opened up a whole new field of research into the pathogenic mechanisms involved in
controlling infections by this organism.

In addition to these achievements in the field of basic medical research Dr. Wakefield also has found
time to pursue his interest in medical education and is coauthor of two books on basic aspects of internal
medicine. He is at present a Senior Lecturer in Immunopathology in the Department of Pathology in the
University of New South Wales.

The Edgeworth David Medal is awarded by the Society for distinguished contributions by young
scientists, usually under the age of 35, working in Australia and contributing to the advancement of
Australian science. Botn in 1950, Dr. Wakefield has demonstrated already in his career that he has the
potential to become one of Australia's great medical researchers, and indeed that he is a worthy recipient
of this Award.

ANNUAL REPORT OF COUNCIL 83

ARCHIBALD D. OLLE PRIZE

The Archibald D. 011€ Prize is awarded jointly to Mr. David S. King and Dr. Nicholas R. Lomb for
their paper entitled "Sydney Southern Star Catalogue".

Mr. King and Dr. Lomb have been astronomers at Sydney Observatory since 1976 and 1979 respectively.
From 1964 the Observatory was engaged in a programme of photographing a large section of the southern sky
to form an astrometric star catalogue. By 1982 the area from -36 declination to the South Pole had been
photographed but only a portion of the plates had been measured.

The decision of the New South Wales Government in 1982 to cease astronomical research at Sydney
Observatory made it necessary to terminate the measurement and reduction of the plates by June 1983. The
resulting catalogue of positions and proper motions of stars was made possible by the energy and
initiative of the two authors, using the New South Wales Public Service computer. The catalogue is
available in magnetic tape and microfiche form. It covers the area from -51 to -65 declination and is
a very valuable contribution to positional astronomy in the southern sky.

OBITUARIES

ROBERT JOHN WALSH

Emeritus Professor Robert John Walsh the Second Dean of the Faculty of Medicine, University of New
South Wales died on 20th July, 1983, at the age of sixty six.

Professor Walsh was born in Brisbane in 1917 and educated at the University of Sydney, graduating
M.B., B.S. in 1939. Asa young resident medical officer at Sydney Hospital Dr. Walsh was invited to fill
the position of Medical Officer-in-Charge in order to supervise the bleeding of donors and preparation of
serum for the new Red Cross Society Service while the Hospital granted him three months leave. This
temporary situation led to Dr. Walsh being appointed Director of the New South Wales Red Cross Blood
Transfusion Service, a post he filled with distinction for a quarter of a century. Under his leadership
this fledgling Service grew from small beginnings in 1941 to a service not only collecting thousands of
blood donations but also offering widening scope of service in serology, biochemistry and haematology
techniques and in the range of blood products supplied. He introduced new modalities of treatment, was
- the co-author of a book on the subject of blood transfusion and had over a hundred research publications to
has credit

Dr. Walsh enlisted for active service during the last World War, was commissioned in the Army and
subsequently posted as the officer commanding the newly created Australian Blood and Serum Preparation Unit
of the Army in Sydney. It was here that he served during the remaining war years as Major Walsh. After
the War he was invited to become the first Director of the New South Wales Red Cross Blood Transfusion
Service.

His formal association with the University of New South Wales commenced in 1962 when he was appointed
visiting professor of human genetics which became a full-time appointment in 1967. He was Chairman of the
Professorial Board of the University in 1970-1973 and member of its Council 1969-1973. He was appointed
Dean of the Faculty of Medicine in 1973, the Second Dean from the foundation of the Faculty of Medicine, a
post which he held until his retirement last year on 3rd January, 1982.

He was a Fellow of the Royal Australian College of Physicians (1955), the Royal College of Pathologists
of Australasia (1956) and the Australian Academy of Science (1958).

He was active in a large number of organizations and held significant executive positions in
committees and societies concerned with haematology and the environment. He was a member of the Council
of the Australian Academy of Science 1963-65 and 1966-70, and of Macquarie University since 1976. His
advice was sought on many issues by both private institutions and government and he gave time and effort
unstintingly to each sector of the community. He served on the advisory committee of the Kanematsu
Institute of Sydney Hospital and was a loyal supporter of this Hospital. He contributed to the framework
of the Institute of Human Biology, Papua New Guinea as Chairman of the Council.

He married Dr. Helen Tooth on 5th June, 1944 and had three sons and one daughter.
He was appointed an Officer of the Order of Australia in 1976 and raised to the rank of Companion
in 1982. For his contribution to the practice and theory of blood transfusion and his work for the

improvement of the environment Professor Walsh was awarded the James Cook Medal of the Royal Society of
New South Wales in 1980.

B.A. Warren

84 OBITUARIES
RAYMOND AUGUSTINE BURG

Raymond Augustine Burg, a member of the Royal Society of New South Wales since 1960, died suddenly on
6th October, 1983, at the ase of 59.

Mr. Burg was born at Maitland on 24th January, 1924, was educated at Marist Brothers' High School,
Maitland, and was awarded ASTC (Chemistry) from Sydney Technical College in 1947. His first position was
as Laboratory Assistant at Elliotts and Australian Drug Company Pty. Ltd., 1942-48. He was appointed
Analyst at the Chemical Laboratory, N.S.W. Department of Mines in 1948, and Senior Analyst in 1960. He
was in charge of the Ceramic Section of the Chemical Laboratory from 1952 until his appointment as Chief
Analyst in 1974, a position he held until thiseretirement in 71982.

Mr. Burg was an authority in the field of clay and ceramics, his work receiving wide recognition in
universities and industry.

Mr. Burg was heavily involved in community activities having an active involvement in school
committees, local clubs and Randwich Roman Catholic Church. He is especially remembered for his caring
nature and consideration of others.

He is survived by his wife and four children.

John McGlynn

MARCEL AUROUSSEAU

One of Australia's most honoured geographers, Marcel Aurousseau, MC, CdeG, BSc (Hons, Syd), Hon
DLitt (Newcastle), died in Sydney on 22nd August, 1983, at the age of ninety-two. Born in Sydney on 19th
April, 1891, he graduated in geology from Professor Edgeworth David's department and went to the University
of Western Australia as assistant lecturer in geology. After a few months in Perth he enlisted in the
A.I.F. and served in Egypt and France. He returned to Perth in 1919 as lecturer in charge of geology but
shortly moved to the Carnegie Institution of Washington to engage in petrological research. An interest in
geography having steadily grown and displaced that in geology, he began to publish on geographical matters
and took a post with the American Geographical Society. In the mid-1920s he travelled considerably, with
very limited funds. He walked from Paris to Madrid and wrote a book, 'Highway into Spain', both descriptive
and interpretive, from his observations. Later he joined the staff of the Royal Geographical Society in
London and then became secretary to the British Permanent Committee on Geographical Names. For more than
two decades he investigated the best methods of rendering geographical names until he 'retired' in 1956.

Aurousseau then returned to Australia and a new generation of Australians came to know and appreciate
his qualities of mind and personality and draw upon his experience. He contributed substantially to the
advancement of Australian academic geography and was from 1964 to 1968 a member of the National Committee
for Geography, of the Australian Academy of Science. With unflagging energy he collated, translated and
edited the letters of the explorer Ludwig Leichhardt, partly to correct what he considered to have been a
misinterpretation by others of Leichhardt's character. The resulting three volumes were published by the
Hakluyt Society in 1968.

Mr. Aurousseau was elected a member of this Society on 1st October, 1919, and was thus in his sixty-
fourth year of continuous membership when he passed away - a record surpassed by few. He contributed two
papers to the Journal, both on ocean temperatures.

He was highly regarded in Australia and overseas and much further information about his life and
publications may be read in R. Freestone's "Marcel Aurousseau and the True Tint of Geography" (Australian
Geographer, 15(1):1-7, 1981), obituaries in the Geographical Journal, 150(1):149-150 and the Australian
Geographer 16(1):1-3, and a full bibliography in the Australian Historical Geography Bulletin.

A.A. Day

NOTICE TO AUTHORS

A “Style Guide to Authors” is available from the
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GENERAL
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PRESENTATION OF INITIAL MANUSCRIPT
FOR REVIEW

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Spelling follows “The Concise Oxford Dictionary”.

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All stratigraphic names must conform with the Inter-
national Stratigraphic Guide and must first be cleared with
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Abbreviations of titles of periodicals shall be in
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1S04 “International Code for the Abbreviation of Titles of
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receive a number of reprints of his paper free. An author who
is not a member of the Society may purchase reprints.

iain

3 9088 01308 4892

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Contents

VOLUME 117, PARTS 1 and 2

GOODWIN, Terence J.. VAGG, Robert S. and WILLIAMS, Peter A.
Chiral Metal Complexes. Part 15. Alanine and Proline Complexes of

[N,N -Di(2-picolyl)-1 R, 2R-diaminocyclohexane] cobalt (111) ]
LINDLEY, I. D.

Stratigraphic Revision of the Early Carboniferous Flagstaff Formation,

Southern New England Belt, N.S.W. oe

OSBORNE, R. A. L. 7 |
Multiple Karstification in the Lachlan Fold Belt in New South Wales:.
Reconnaissance Evidence 15

MARTIN, Helene A.
The Stratigraphic Palynology of the Murray Basin in New South Wales. II.
The Murrumbidgee Area 35

MARTIN, Helene A.
The Stratigraphic Palynology of the Murray Basin in New South Wales.
III. The Lachlan Area 45

COOK, J. L., ROSE, E. K. and CLANCY, B. E. 7
Computation of Reaction Matrix Parameters by Perturbation Theory 53

VLAARDINGERBROEK, Barend
Notes on Freshwater Zooplankton Found in Central Province,
Papua New Guinea, 1981-2 63

JONES, Hon. Barry O.
Changing Employment Patterns and Truncated Development in Australia
(Address on the Occasion of the Annual Dinner of the Royal Society of

N.S.W., 21st March, 1984) 67
ANNUAL REPORT OF THE COUNCIL FOR THE YEAR ENDED 3lst
March, 1984 71

Publicity Press (NSW), 66 O'Riordan St, Alexandria, Sydney.