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For further information contact the University’s Copyright Service. sydney.edu.au/copyright A BIOSTRATIGRAPHY OF THE LATE PERMIAN

AND TRIASSIC OF THE SYDNEY BASIN

(VOLUME 1)

Robin Helby

A thesis submitted to the University of Sydney as partial requirements for the Degree of Doctor of Philosophy, -ii-

TABLE OF CONTENTS

VOLUME 1

ABSTRACT iv

1. INTRODUCTION

1.1 General 1

1.2 Material 3

1.3 Preparations 6

Storage 7

Records 7

1.4 A Review of Australian "Triassic" Palynology 7

2. OBSERVATIONS 29

2.1 Stratigraphy 29

2.2 Descriptive Palynology 54

Sys tematics 56

VOLUME 2

2.3 The microfloral sequence of the Sydney Basin 301

Dulhuntyispora Assemblage Zone 301

Protohaploxypinus retioulatus Assemblage Zone 305

Lunatisp orites pelluoidus Assemblage Zone 312

Protohaploxypinus samoiloviohii Assemblage 320

Zone

Faloisporites Assemblage Zone 328

3. COMPARISONS AND INTERPRETATIONS

3.1 Comparisons of Sydney Basin Assemblages with

other microfloras 340 - i ii-

Dulhuntyispora Assemblage 343

Protohaploxypinus vetioulatus Assemblage 350

Lunatispovites pelluoidus Assemblage 360

Protohaploxypinus samoiloviohii Assemblage 368

Falo'isporites Assemblage 379

3.2 An Environmental Synthesis 392

Acknowledgements 404

References 406

Appendix 1 - Sample Data 446

PLATES VOLUME 3 iv-

ABSTRACT

The stratigraphic framework of the Late Permian to Triassic sequences which comprise the upper coal measure successions, the

Narrabeen Group, the Hawkesbury Sandstone, Wianamatta Group and equivalent strata in the Sydney Basin is outlined together with a brief summary of the available biostratigraphic information.

The vertical distribution of microfossils from 252 samples, arranged in 14 sample sequences, is illustrated. Taxonomic treatment of 119 species comprising 74 genera of spores and pollen is undertaken and 19 species of microplankton are briefly described. Nineteen species and three genera are proposed as new taxa.

On the basis of the vertical distribution and relative prominence of the described palynomorphs five assemblage zones are delineated. These are in descending order,

1. The Faloisporites Assemblage Zone (four zonules identified)

2. The Protohaploxypinus samoiloviohii Assemblage Zone

3. The Lunatisporites pelluoidus Assemblage Zone

4. The Protohaploxypinus retioulatus Assemblage Zone

(two zonules identified)

5. The Dulhuntyispora Assemblage Zone.

The Dulhuntyispora Assemblage Zone occupies the coal measure sequences below the base of the Narrabeen Group, The junction of the Dulhuntyispora Assemblage Zone and the Protoha ploxypinus retioulatus Assemblage Zone is coincident with the base of the Narrabeen Group, the latter zone occurring in the lower part of the Narrabeen Group. The Lunatisporites pelluoidus -v-

Assemblage Zone and the Protohaploxypinus samoiloviohii Assem

blage Zone, which exhibit essentially homotaxial microfloras,

occupy the central portion of the Narrabeen Group succession,

The Faloisporites Assemblage Zone extends from the upper portion

of the Narrabeen Group, through the Hawkesbury Sandstone to the

top of the Wianamatta Group, However, the Lunatisporites pellu-

oidus Assemblage has not been encountered in the northwest

portion of the basin.

The microfloral sequence of the Sydney Basin compares

closely with other Gondwana occurrences, particularly those of

Western Pakistan and Madagascar. The individual assemblages are

examined in terms of equivalent microfloras from a number of

phytogeographic provinces.

Environmental synthesis suggests that the base of the Narra been Group coincides with a substantial erosional hiatus. The

environment of deposition of the sediments above the hiatus is

interpreted as brackish or shallow marine on the basis of the geometry of the basal sequence and the occurrence of a diverse and abundant acritarch assemblage, Evidence of the co-existence of the floras represented by the Lunatisporites pelluoidus

Assemblage, the Protohaploxypinus samoilovichii Assemblage and

the Faloisporites Assemblage is illustrated and an interpretation of the environments of the individual floral communities is attempted. Despite meagre data, an erosional Hiatus is indicated between the top of the Narrabeen Group and the Hawkesbury Sand stone. The contemporaneous deposition of the Hawkesbury Sand stone and the Ashfield Shale is discussed, The similarity of -vi-

the microfloras of these formations, together with their mutually adjacent depositional areas is interpreted as supporting the concept of a tidal delta-barrier bar origin for the Hawkesbury

Sands tone.

150° OUTCROP OF SEDIMENTS

NARRABRI ASSOCIATED WITH

THE SYDNEY BASIN

DUBBO

PORT STEPHENS

BRISBANE STUDY AREA

KILOMETRES 10 0 10 20 30 40 50 60 70 80

GEOLOGICAL SURVEY OF N S * DEPARTMENT OF MINES 5106 - 1 -

INTRODUCTION

1.1. GENERAL

The Sydney Basin is the modified remnant of a

N.N.W. trending trough in which a thick sequence of

Permian and Triassic rocks accumulated. In its present

form it extends along the coastline from Durras Lake

in the south to Port Stephens in the north. The east

ward extension as part of the continental shelf is yet

to be fully delineated. The western margin extends from

Durras Lake to Ulan, the basal sediments resting uncon-

formably on Lower or Middle Palaeozoic metasediments and

granites. From Ulan the western margin swings west to

Dubbo, north of which it passes below a thin Jurassic

cover. The north-eastern margin extends from Port

Stephens more or less paralleling the Hunter Thrust

system to the vicinity of Narrabri. To the north and

west of Narrabri the limits of the Sydney Basin below

the Jurassic and Cretaceous cover are uncertain although

sedimentation was probably intermittently continuous with

similar sequences in Southern Queensland.

Synthesis of available data suggests a maximum thick

ness of the Sydney Basin sequence in excess of 18,000 ft.

The Early to Mid Permian portion of the sequence is com

prised essentially of marine shelf and deltaic sediments

with a major fluvio-deltaic development at the top. It

has a maximum composite thickness of about 15,000 ft. - 2 -

The marine sediments of this section contain rich invertebrate faunas while the fluvio-de1taic environ ment is represented by the extensive and abundant

Glossopteris flora. The overlying Late Permian to

Triassic sequence, on which this study is based, com prises fluvial, fluvio-deltaic and shallow marine sediments which have a maximum composite thickness of about 4,000 ft. Invertebrate remains are extremely rare while floral assemblages are both localised and sporadic, inhibiting the development of a biostratigraphy.

The aims of this study are:-

1. to determine and describe the principal components

of Late Permian-Triassic microfloras of the Sydney

Basin.

2. to delineate consistent microfloral associations and

analyse their distribution and interrelationships.

3. to compare these assemblages and the overall palyno-

logical sequence to other Late Permian-Triassic micro

floras .

This study was initiated in 1960 to establish a biostratigraphic framework to accompany a lithostratigraphic division of the Narrabeen Group in the Burragorang area. This early investigation established the presence of diverse and abundant microfloras in that area and indicated their potential stratigraphic significance. In

1963 the project was expanded to encompass the present - 3 -

objectives. The investigation was suspended in December,

1963, and recommenced during 1967 in conjunction with a

study of the Sydney Basin by the New South Wales Geological

Survey.

1.2. MATERIAL

Microfloras were recovered from 228 of the 277

samples processed as part of this study. In addition

10 of the original preparations from Appin D.D.H.No.4

(samples 682-691) investigated by Hennelly (1959) were

reprocessed. Slides of 14 preparations from Terrigal

D.D.H.No.l were kindly provided by Dr. P.R. Evans.

Preparations of 201 samples from the Narrabeen Group

were examined. Of these 183 were arranged in 9 strati

graphic sequences which included eight diamond drill cores

and a well catalogued selection of material from the Bal

main Shaft. Seven of these sections including 159 samples

are located on Figure 2. They are from north to south -

1. Ourimbah Creek D.D.H. No.5 (50 s amp1e s)

2 . Ourimbah Creek D.D.H. No.4 ( 3 samp 1e s)

3 . Terrigal D.D.H. No.1 (14 samp 1e s)

4 . Balmain Shaft (13 s amp 1e s)

5 . Camden D.D.H. No.61 (44 samp1e s)

6. Appin D.D.H. No. 4 (basal 80 ft . ) (10 s amp1e s)

7 . Wollongong D.D.H. No. 28 (25 samples) - 4 -

Quality of the preparations varied considerably within each sample series. However, the state of pre

servation of microfossils generally improved to the

north and west of the Appin-Wo1longong area where

carbonisation of exines was intense. Preservation

noticeably improved in higher portions of most Narra-

been Group sections.

Preparations of 18 samples of Hawkesbury Sandstone

sediments were examined, 10 of these representing a

single sequence from Wollongong D.D.H. No. 28. The

state of preservation of the microfloras in this sequence varied considerably. 32 samples from the Wianamatta

Group were processed. These were collected from scattered

localities, mainly comprising shallow excavations and

road cuttings. The shallow location of many samples was

reflected in the poor quality of the preparations. 44

samples from the Wollar Sandstone and its equivalents in

the northern portion of the Sydney Basin (see Table 1) were examined. 22 of these samples were collected in 3

stratigraphic series.

1. Quirindi D.D.H. No. 1 and Poggy D.D.H. No. 1

(9 samp les)

2. Mirrabooka D.D.H. No. 1 (4 samples)

3. Cutting at eastern end of Cox’s Gap Tunnel - 80 ft.

section. (9 s amp les) - 5 -

The majority of other samples from this area were taken

from seismic shot hole cutting piles (?bottom hole samples)

and consequently have a limited biostratigraphic relia

bility. The quality of preparations from this north

western area is generally fair with a relatively low

degree of carbonisation.

Reference details of samples are set out in Appendix

1. Unless otherwise indicated the geographic location of

the sample is presented as a grid reference taken from the

1 Mile military map series. Rock unit names assigned to

samples from D.M. Camden D.D.H. No. 61 and D.M. Wollongong

D.D.H. No. 28 follow Brunker (in press) and Wood et aZ.

(1963). Formation names indicated for samples from Terrigal

D.D.H. No. 1, Ourimbah Creek D.D.H. No. 4 and No. 5 conform

to the nomenclature proposed by Stuntz (in preparation).

Samples taken from outcrop are noted by means of an asterisk

following the description of the lithology. The relative

state of preservation of the microflora of each sample is

described as very poor, poor, fair or good. In samples

of very poor preservation the majority of specimens are

not identifiable at species level. Poor preservation denotes

samples in which the majority of specimens are identified

with difficulty at specific level. Fair preservation

indicates that the majority of specimens are easily

identified. - 6 -

1.3. PREPARATIONS

The microfloras were extracted from the sediments

by conventional techniques. Crushed sediment, other

than coal, was boiled with commercial hydrofluoric acid

(70%) and the resultant complex fluorides were dissolved

by boiling in dilute hydrochloric acid. The remaining

mineral matter was separated by centrifuging with a

bromoform/alcohol mixture or zinc bromide so lut ion(S.G. 2.1).

Although the bromoform/alcohol mixture produced cleaner

separations, the application of zinc bromide solution was

more rapid. A smear of organic residue was examined to

estimate the required time of oxidation treatment.

Samples 626 - 645 were not oxidised by Schulze solution -

alkali treatment. Partial cleaning of these samples was

affected by repeated chlorination (for description see

Erdtman 1943, p.29). Oxidation of the majority of samples

consisted of conventional Schulze solution - alkali treat

ment (time of oxidation ranging from 3-25 minutes). Later

samples were treated by the modified technique described

by Playford and Helby (1968, p.106).

Coal samples were processed by conventional Schulze

solution - alkali treatment. Time required for oxidation

was assessed by constant checking of the residue. Mineral

matter was removed by gravity separation (described above).

The microfloral residues were mounted in glycerine

jelly. The number of slides of each sample varied, although - 7 -

at least two strew slides were prepared, except where

insufficient residue was recovered.

STORAGE

All slides and residues (apart from residues bearing

Bureau of Mineral Resources and C.S.I.R.O. sample numbers)

are stored at the Mining and Geological Museum, Sydney.

RECORDS

Data concerning the microfloral composition of each

sample are recorded on individual sample cards. The

location of at least one specimen of each species is

noted, although obviously prominent species are noted

but not always located. These sample cards are the basic

data from which distribution charts are established. Details

from the sample cards are also transferred to individual

species cards. Species cards often record additional data

concerning the actual specimens on which the concept of

these species is based.

1.4. A REVIEW OF AUSTRALIAN "TRIASSIC" PALYNOLOGY

A considerable amount of generally available data

concerning Late Permian-Triassic microfloras has accumu

lated over the past decade. These data suggest a unifor

mity of microfloral sequential patterns, particularly in

eastern Australia. The first comprehensive synthesis is

contained in the palyno-stratigraphic framework of Eastern

Mesozoic strata proposed by Evans (1966). Evans delineated - 8-

three informal palynological units (microfloral stages),

including eight microfloral assemblages, ranging in age

from Late Permian through Triassic. These proposals have

been widely and successfully applied although there is now

obvious need for a number of revisions.

The earliest published investigation of Australian

Triassic plant microfossils is that of de Jersey (1949).

This study included descriptions of 31 microfossil "types"

from coals of the Ipswich Coal Measures of southern Queens

land. The microfossils were classified according to the numerical system outlined by Dulhunty (1945) and were

illustrated by line diagrams. Recognisable genera include

Falcispovites (type 38A) Circulisporites (type 25A) and

Cycadopites (type 8A). De Jersey (1949, p.6) indicated

that 35 percent of the species occuring in the Ipswich assemblages were conspecific with elements previously reported from local Permian microfloras. On the basis of this observation de Jersey suggested that the Ipswich microflora was possibly older than Mid-Triassic as indi cated by plant megafossils. Of the 145 spore "types" recognised in microfossil assemblages from the Leigh Creek

Coal Measures, South Australia descriptions of 62 were presented by Taylor (1953). Taylor applied Dulhunty1s numerical classification and illustrated the forms with interpretative line diagrams. Recognisable species include

Dictyophyllidites mortcni (type 2C), Cycadopites sp. (type

3A), Neoraistriokia taylori (type 19 B), Osmundacidites sp. - 9 -

(type 29B), Endosporites radiatus (type 34C) and

Faloisporites spp. (type 38-40). Taylor’s investi gation was undertaken to facilitate local coal seam correlation and although strong similarities with the microflora of the Ipswich Coal Measures were obvious the author made no speculations concerning the age of the sequence.

The first formal descriptions of plant microfossils assigned to the Triassic System in Australia are those presented by Hennelly (195ft). Hennelly examined the microfloral sequence of the basal Narrabeen Group section immediately above the Bulli Seam (Illawarah Coal Measures) in Appin D.D.H. No. 4. Seven "microspore" species and two megaspore species were described, six of these as formal new species. This microflora was dominated by two bisaccate forms Faloisporites (Fityosporites) nigracristatus and Protohaploxypinus (Pityosporites)retioulatus (Hennelly's concept includes P. miorooorpus). Hennelly recognised a number of forms characteristic of the underlying coal measure microflora (Dulhuntyispora assemblage of Balme,

1964). On this basis he proposed a thin Permian-Triassic transition zone, characterised by Quadrisporites horridus

(now recognised as an acritarch) and Apioulatisporis bulliensis. The section above 1696 ft. was assigned to the Triassic.

Megaspore assemblages from the Leigh Creek Coal Mea sures and the New Town Coal Measures of Tasmania have been - 10 - described by Dettmann (1961). Dettmann reports an assemblage comprised of Nathors tisporites including

N. hoplitious and N. retioulatus from the Leigh Creek material. She indicates that N. hoplitious is confined to Rhaetic and lower Liassic strata of East Greenland and assigns a similar age to the Leigh Creek assemblage. The

Tasmanian assemblage was more diverse and was characterised by Banksisporites pinguis and Nathorstisporites flagellatus.

The presence of Banksisporites pinguis was interpreted by

Dettmann as indicating a correlation with the Rhaetic

(Lepidopteris Zone) of Greenland. However, Dettmann was properly cautious in applying this age due to the simi larity of B. pinguis to megaspores of the Early Triassic

Selaginellites polaris.

The distribution of the Striatiti in Australia and their relationship to the Glossopteris flora was discussed by Balme (1960). In this account (p. 276) he recorded

Lunatisporites ( = " Lueekisporites"=Taeniaesporites) from the Narrabeen Group. Helby (1962 - unpublished) dis cussed the palynological sequence of a Narrabeen Group section in the Burragorang area. Three microfloras were delineated. The lower of these compared directly with the microflora described by Hennelly (1959) from Appin.

It was however, considerably more diverse. The second microflora extended from the upper part of the Caley

Formation and included most of the lower member of the

Grose Sandstone. It was characterised by forms best - 11- ass igned to Lunatisporites (= Taeniaesporites)3 Proto- haploxypinus miorooorpus and Striomonosaooites spp. This assemblage was compared directly with Late Permian micro floras of western Europe. The upper microflora was characterised by Lunatisporites and a diagnostic pteridophytic assemblage and occupied the remainder of the Grose Sandstone. Aratrisporites was not recognised in this assemblage. This microflora was equated with the

Lower Triassic microflora of the Kockatea Shale, On the basis of these wide ranging correlations Helby suggested that the section containing the lower two microfloras should be regarded as Permian in age.

In an essentially systematic work de Jersey (1962) presented formal descriptions of 33 species from the

Ipswich Coal Measures. These superseded the informal numerical classification applied by de Jersey (1949).

In this paper de Jersey drew attention to the relation ship of Faloisporites (=Alisporites) and the corystospermaceous plants which characterise the Dicroidium flora. Unfortunately quantitative data concerning the various species was not usually included. This was followed by a study of the microflora of the overlying

Bundamba Group (de Jersey, 1964). In this later work de Jersey indicated that the microfloras of both the

Ipswich Coal Measures and the Bundamba Group are domi nated by Faloisporites with prominent Polypodiisporites ipsviciensis3 Converruoosisporites earneroni and Puncta- tosporites walkomi. It was further indicated that - 12-

T enuisaccites fragiZis and PerotriZetes (CinguZati -

sporites) paZZidus are restricted to the Ipswich Coal

Measures while CircuZina meyeriana3 Foveosporites moretonensis 3 Dis cisporites verrucosus 3 Partitisporites novimundanus3 TubercuZatosporites abadarensis3 Lycopo-

diumsporites antiquus and Vitreisporites microsaccus did not occur below the base of the Bundamba Group. It

is interesting to note that Aratrisporites was not reported from either assemblage. On the basis of the European

distribution of Partitisporites3 DupZicisporites and

CircuZina de Jersey suggests a Karnian to Norian age for the Bundamba Group.

The study of the microflora of the Kockatea Shale from the Perth Basin, Western Australia (Balme 1963) is particularly significant to the understanding Australian

Triassic microfloras. The basal member of the Kockatea

Shale, a calcareous siltstone, contains a marine fauna consisting of ammonites, pelecypods, lingulid brachiopods and conchostrachans which establish its age as lowermost

Scythian. Balme described a well preserved microflora which occured in association with the marine fauna. The

assemblage was characterised by Lunatisporites and dominated by a group of lycopsid microspores which have been assigned to PerotriZetes (=KraeuseZisporites) Lund-

bZadispora and Densoisporites. Microplankton were abundant

in all samples, WiZsonastrum (=Veryhachium) being identified as the dominent genus. Densoisporites (=LundbZadispora) - 13-

playfordi was the dominent spore form. This assemblage

was later designated as the"Taeniaesporites" microflora

(Balme,1964). Balme outlined the world wide distribution

of "Taeniaesporites" postulating a vast phytogeographic

province which included Australia and Madagascar. He

suggested that the advent of this assemblage including

"Taeniaesporites"in the province could be interpreted as

an Eo-Triassic event. In discussing the Australian dis

tribution of "Taeniaesprorites" Balme cited an occurrence

at the base of the Narrabeen Group in the Nattai River

district (=Burragorang area). The work of Helby (1962)

suggests that this sample should be located some distance

above the base of the sequence.

Playford & Dettmann (1965) presented results of an

investigation of the microflora of the Leigh Creek Coal

Measures, South Australia. These authors formally des

cribed 28 species and identified a further seven species

of plant microfossils. Of these 13 had been previously

recognised by Taylor (1953). The presence of a Jurassic

sequence above the previously described Triassic section was indicated by the abundant occurrence of Ctas sop oilis olassoides in samples from the Telford Basin. The Triassic

section contained an abundant and diverse microflora which was more or less dominated by Faloisporites (=Alisporites) with locally prominent Polypodiisporites ipsviciensis and

Converruoosisporites cameroni. Significant accessory genera

included Aratrisporites3 Duplexisporites and Polycingu- - 14- latisporites. This latter form was more prominent in the Jurassic sequence. Although the European ranges of number of individual species were dicussed the occurrence of the megaspore Nathorstisporites hoplitious3 previously interpreted by Dettmann (1961), was considered to preclude a pre-Rhaetic age for the Triassic assemblage.

The results of a palynological reconnaisance of the

Triassic of the northern Tasmania Basin were presented by

Playford (1965). Six productive samples, one from the basal Ross Formation, two from the Tiers Formation and three from the Brady Formation and its probable equiva lents were discussed. The assemblages recovered from these samples suggest that the formations involved could be readily distinguished by their palynological content.

The Ross Formation assemblage was characterised by

Protohaploxypinus samoiloviohii3 Lundbladispora spp.,

Perotriletes ouspidus and Densoisporites playfovdi.

Playford noted the absence of Lunatisporites in comparing this assemblage to Early Triassic microfloras of Western

Australia. If the absence of Aratrisporites is confirmed by further sampling this microflora can be confidently equated with central portions of the Narrabeen Group. The microflora of the Tiers Formation was dominated by Aratri- sporites spp. and Faloispovites spp. with a prominent

Protohaploxypinus samoiloviohii component. This micro flora is reminiscent of assemblages from the upper part of the Narrabeen Group in the Sydney Basin. The micro- - 15- floras recovered from the Brady Formation and its equivalents are dominated by Faloisporites spp. The occurrence of Cyeadopites nitidus and Aratrisporites parvispinosus in the assemblage may be stratigraphica1ly significant. Playford suggested a Late Triassic, probably Rhaetic age for the formation.

Microfloral data concerning the Mount Crosby

Formation of the Ipswich Coal Measures is discussed by de Jersey & Hamilton (1965a). This paper extended the known range of Duplexisporites gyratus and Dis- aisporites verrucosus. The authors indicated that the

Ipswich Coal Measures are younger than the Moolayember

Formation on the basis of the absence of Polyeingulati- sporites densatus in the latter formation. These same authors recorded microfloras from the Moorooka and

Tingalpa Formations of the Brisbane area (de Jersey &

Hamilton, 1965b). The assemblages were dominated by

Faloisporites spp. with prominent 0smundacidites sp. and Polypodiisporites ipsvioiensis . Duplexisporites gyratus was common in most assemblages. The presence of Tenuisaocites fragilis and Perotriletes pallidus in the assemblages prompted the authors to propose a cor relation with the Ipswich Coal Measures. The association of microfloras of this age with comtemporaneous vulcanism may be significant in comparisons with sequences in other basins.

Helby (1967) described the microflora of a single - 16-

sample from the central portion of the Wollar Sandstone,

N.S.W. Fifteen species of microspores and pollen and one megaspore species were reported. The assemblage was dominated by Aratrispori-tes (see description of A. tenuispinosus)jFaloispovites and Osmundaoidites. Diagnostic forms included "Nevesisporites" limatulus (=Retusotriletes olipeata) and Perotviletes differens. Cyoadopites was not recorded. Helby suggested that Aratrisporites is an important biostratigraphic form. He discussed the dis tribution of this genus, concluding that it first appears in late Scythian stata at widely separated localities throughout the world. He also indicates that the assem blage compared closely with uppermost Narrabeen Group microfloras and suggested a late Scythian or lower Anisian age .

Permian - Triassic sedimentation in the Sydney Basin was more or less paralleled by deposition of a similar sequence in the Bowen Basin of Southern Queensland. The upper three formations of the Bowen Basin succession com prise in ascending order the Rewan Formation, the Clematis

Sandstone and the Moolayember Formation. These units are generally assigned to the Triassic. There is perennial disagreement concerning the age of the Rewan Formation, some of the major contributions to the discussion being outlined by Evans (1963). The southern extension of this outcrop sequence below sediments of the Surat Basin have been recognised in the Cabawin Formation and the overlying - 17-

Wand o an Formation. The exact relationship of these two

subcrop formations to the outcrop sequence is presently

uncertain.

An abundant and diverse microflora from the Moola-

yember Formation is described and analysed by de Jersey

& Hamilton (1967). These authors recorded 60 species of

spores and pollen, including two forms which could be

regarded as acritarcha. The microflora was generally

dominated by Faloisporites with prominent 0smundaoidites

and Cycadopites. Potentially important stratigraphic

forms include Cadargasporites senectus3 Apioulatisporis

(=Verrucosisporites) oarnarvonensis and Protohaploxypinus jaoobii. The known ranges of a number of forms including

Duplexisporites gyratus3 "Nevesisporites " limatuluss Pero- triletes differens (=Kraeuselisporites verruoifer) Tuber- oulatosporites abadarensis3 Discispovites psilatus and

D. verrucosus were extended. The authors referred to the effect of facies on the quantitative distribution of

Perotriletes differens3 Foveosporites mimosae3 Rugulati- sporites stonecrofti and Aratrisporites "plicatus"j although definite patterns were not established. In an analysis of the vertical distribution of forms the authors

suggest that Lophotriletes bauhinae3 Aratrisporites sp.cf.

A. rotundus} Tigrisporites play fordi and Rugulatisporite s trisinus are confined to the lower portion of the formation.

In comparing the microflora of the Moolayember Formation

to assemblages from other units de Jersey & Hamilton - 18- main t ained their previously stated opinion concerning

the relationship of the Ipswich Coal Measures (de

Jersey & Hamilton, 1965a). They considered that the absence of Polycingulatisporites densatus 3 Annulispora folliculosa and A. micro annul at a from Moolayember Forma

tion assemblages indicated that the formation is older

than the Ipswich Coal Measures. It should be noted that

the published occurrences of these species (apart from

the report of P. densatus in carbonaceous shale from the

Mount Crosby Formation) in the Ipswich Coal Measures are recorded from microfloras extracted from coals. Of the

78 samples recorded in the Moolayember study only three were comprised of coal and it is extremely doubtful if the environment of deposition of the respective coals could be regarded as similar. The Moolayember Formation assemblage was also compared with the Triassic portion of the Leigh Creek microfloral sequence (Playford & Dettmann,

1965), the authors concluding that the latter occurrence was younger. This was based on the occurrence of P. densatus and the absence of some typical Moolayember species in the Leigh Creek material. The same argument was applied to the comparison with the Brady Formation and "Feldspathic Sandstone" microfloras of northern Tas mania (Playford, 1965). De Jersey & Hamilton suggest a

Mid Triassic Age for the Moolayember Formation, based on synthesis of the ranges of a number of individual European species. - 19 -

The microflora of the Clematis Sandstone was described by de Jersey (1968). Fifty three species were identified in a microflora dominated by Falcisporites with prominent Osmundacidites 3 Leiotviletes and Sterei- sporites components. Distinctive forms reported for the first time from Australian sequences include Guttatisporites vis scheri 3 Indospora clara and Equisetosporites steevesi. De Jersey indicated that the microflora of the Clematis

Sandstone is essentially similar to that of the overlying

Moolayember Formation, although Duplexisporites gyratus and Cadargasporites senectus appeared to be confined to the upper unit. The quantitative data suggest that Aratrisporites was more common in the upper part of the formation. This paper also included some data concerning uppermost Rewan Formation microfloras (see Fig. 3). The assemblage was dominated by Falcisporites and Osmundacidites with prominent Leiotviletes and Aratrisporites tenuispinosus. It is interesting to note the presence of Cycadopites nitidus in the assemblage. Evans (1963, 1966) indicates that restricted basal portions of the Rewan Formation con tain an assemblage directly comparable to, although considerably more diverse than, the basal Narrabeen Group microflora described by Hennelly (1959). He suggested that these lower horizons of the formation are restricted by an onlapping unconformity, above which the "Taeniae- sporites" microflora of Balme (1964) extended through the greater part of the formation. Microfloras in the upper- - 20- most portion of the formation were dominated by

Faloisporite s and characterised by several species of

Aratrisporites.

There exist numerous records of microfloral assem blages extracted from sediments assigned to the Wandoan

Formation. These are found mainly as appendices to published and unpublished well completion reports con cerning petroleum exploration in the Surat Basin. De

Jersey & Hamilton (1969) presented a compilation of their data from twelve wells. They indicated a two fold division of the microfloral lists, the lower being compared with microfloras from the lower and central portions of the

Clematis Sandstone. The upper group was equated with assemblages from the upper part of the Clematis Sandstone and the lower portion of the Moolayember Formation. The authors noted the presence of Buplexisporites gyratus and

Cadargasporites senectus in a sample which on lithostratigraphic evidence is placed 230 ft. below the top of the

Clematis Sandstone. This considerably extended the pub lished range of these species. Assemblage lists from

Cabawin Formation samples were confined to well completion reports. Evans (1963 - unpublished) correlates the Cabawin

Formation in U.K.A. Cabawin No. 1 with the Clifton Sub group of the Narrabeen Group and includes the uppermost portion of the Newcastle Coal Measures. This would suggest a microfloral sequence in the Cabawin Formation ranging from the Dulhuntyispora assemblage to the "Taeniaespovites" - 21- mi c r o f lora .

Helby {in Packham, 1969) reviewed the palynostrati- graphy of the Narrabeen Group of the Sydney Basin (see also Helby, 1969) and outlined the principal microfloral features of the Hawkesbury Sandstone and the Wianamatta

Group. Three major microfloras were recognised in the Narrabeen Group. The description of the major features of these microfloras is reproduced here.

The lowermost microflora was characterised by

"Densoisporites " fibulatus3 Triquitrites proratus3

Apioulatisporis bulliensis 3 Polypodiisporite s ipsvioiensis 3

Punotatosporites waVkomi3 ProtohapZoxypinus sp. cf. P. microeorpus and Quadrisporites horridus with very prominent

Alisporites and Osmundaoidites components. Dulhuntyispora parvithola3 Gnetaceaepollenites sinuosus. Protohaploxy- pinus limpidus and other forms characteristic of the microflora of the underlying coal measures occurred in constant but minor proportions in the lower part of the section occupied by this lower microflora, gradually dis appearing towards the upper limits of the microflora. A restricted zone of occurrence of Lueckisporites singhii had been encountered in this microflora, from a section in the vicinity of Wyong. The microflora has been encoun tered in the Coalcliff Sandstone, Wombarra Shale and the lower portion of the Scarborough Sandstone to the south of Sydney. It occupied most of the Caley Formation to the west and southwest and the shaly lower portion of the - 22-

Munmorah Conglomerate to the north of Sydney.

The advent of the second microflora was marked by the sudden and abundant appearance of Lunatisporite s pelluoidus together with L. noviaulensis. This second microflora may be divided into two assemblages, the lower of which is characterised by very abundant L. pelluoidus3 several species of Striomonosaooites and several large species of Protohaploxypinus. Alisporites was locally abundant but the diverse pteridophytic elements seldom attained prominence. This assemblage occupied the upper most part of the Caley Formation and the lower member of the Grose Sandstone in the Burragorang area and had been recognised in the Scarborough Sandstone and Stanwell Park

Claystone to the south of Sydney. It occupied the upper portion of the Munmorah Conglomerate, extending into the

Tuggerah Formation.

A rapid decline in the prominence of the larger gymnospermous pollen and dominance of pteridophytic forms marked the lower limits of the upper assemblage.

Distalanulisporites 3 Densoisporites, Lundbladispora and

Kraeuselisporites are the dominant pteridophytic elements,

Alisporites and Lunatisporites were the prominent gymnospermous forms. This upper assemblage occupied the upper member of the Grose Sandstone in the Burragorang area, the greater part of the Bulgo Sandstone to the south of

Sydney and has been recognised in the Tuggerah Formation, possibly extending into the Collaroy Claystone to the - 23-

north of Sydney.

The lower limit of the upper microflora was marked

by the first appearance of Aratrisporites. As it occurred in the Narrabeen Group this upper microflora can be divided,

tentatively, into two assemblages. The lower of these

appeared to be inimately associated with the development

of red beds. It was characterised by Densoispor ites playfordi> an unnamed Distalanulisporites (=Limatula-

sporites fossulatus) and several species of Aratrisporites.

Lunatisporites was the dominant pollen form although

Alisporites was increasingly prominent towards the upper

limits of the assemblage. The upper assemblage was domi

nated by Alisporites. Densoisporites was virtually absent

and Aratrisporites occurred in minor proportions. This assemblage occupied the section assigned to the Gosford Formation to the South of Sydney and has been encountered in the upper part of the Gosford Formation to the north of Sydney. It was essentially similar to the microflora

occurring in the Hawkesbury Sandstone.

In discussing the age of the Narrabeen Group Helby

indicated a direct comparison of the second Narrabeen Group microflora to established Early Triassic assemblages reported from the Kockatea Shale of Western Australia and

the Middle Sakamena Group of Madagascar (Goubin, 1965). On

the basis of these comparisons it was suggested that the

Permian-Triassic boundary would be located within the lower limits of this microflora. From the conclusions - 24- above which are supplemented by comparison with the

Tartarian Chhidru Formation of Pakistan, the lower micro flora of the Narrabeen Group was assigned a Permian age.

The appearance of Aratrisporites in uppermost Scythian microfloras at widely scattered localities has been discussed by Helby (1967). This concept was applied to suggest an upper Scythian to early Anisian age for the upper part of the Narrabeen Group.

Microfloral assemblages of the Hawkesbury Sandstone were dominated by Falcisporites spp. with prominent

Osmundaoid.ites3 Cy oadopites and Protohaploxypinus com ponents. Forms regarded as diagnostic of the assemblage included "Nevesisporites" limatulus3 Perotriletes differens and ?Equisetosporites steevesi. Duplexisporites gyratus was reported from the central part of the formation.

Microfloras from the lower portion of the Wianamatta Group are essentially similar to assemblages in the underlying

Hawkesbury Sandstone. "Nevesisporites” limatulus appeared to be limited to the basal portion of the section, Cadar- gasporites (C. seneotus) first appearing in strata assigned to the Minchinbury Sandstone. The intermittent occurrence of acanthomorphitae acritarchs were interpreted as indi cating a brackish or possibly marine environment of depo sition.

General reviews of Australian Late Permian and Tri- assic palynology have been presented by Balme (1964) and

Evans (1966). Both these works are incorporated in more - 25- extensive syntheses. Balme observed that the Upper

Permian spore assemblages which comprised the Dulhuntyi-

spora - Assemblage display remarkable uniformity throughout Australia. This assemblage occupied the Mid-Late Permian coal measures sequences of eastern Australia. The decline

of the assemblage at the top of these sections was generally

accepted as marking the Permian-Triassic boundary. Balme

recognised two microfloras in the Triassic System. The

lower of these, the "Taeniaespovites" - Microflora was

confined to the Kockatea Shale of the Perth Basin and the Blina Shale of the Canning Basin. The microflora was

characterised by Lunatisporites (=Taeniaesporites) and a

characteristic assemblage of lycopsid microspores (subse quently described by Balme, 1963). A sample from near the base of the Narrabeen Group was indicated as containing a relatively high proportion of Lunatisporites3 but differed in other respects from typical "Taeniaesporites" - Micro flora assemblages. It could be speculated that this microflora possibly conformed to the lower portion of the second microflora outlined by Helby (in Packham, 1969).

Rare occurrences of Lunatisporites were also recorded from the upper part of the Narrabeen Group and from coals at Quorn, South Australia, where they are associated with the overlying "Pteruohipollenites" - Microflora.

ThenPtevuohipoltenites " - Microflora replaced the

"Taeniaespovites" - Microflora towards the top of the

Kockatea Shale. This assemblage was characterised by - 26-

Faloisporites (=Alisporites = Pteruchipollenites) which

Balme linked with the corystospermaceous plants comprising the D'icvo'id'ium flora. This microflora was stated to range from the upper portion of the Collaroy Claystone, through the Hawkesbury Sandstone and Wianamatta Group in the

Sydney Basin. It occupies the Ipswich and Callide Coal

Measures of Queensland and was reported from coals at

Leigh Creek and Springfield, South Australia and St. Mary's,

Tasmania. Despite the meagre data available Balme was obviously aware of the complex interrelationships of these

Australian Triassic microfloras.

As stated above the most comprehensive published account of Australian Late Permian-Triassic microfloral patterns is included in Evans (1966). This study deline ated three informal palynological units which were essentially similar to microfloral stages. These were further divided into eight assemblages. The lowermost of these assemblages, Unit Tr la, rapidly replaced the underlying Unit P4 (equivalent to the upper portion of

Balme's DuZhuntyispora Assemblage) at the base of the

Narrabeen Group in the Sydney Basin and in isolated basal sections of the Rewan Formation in the Bowen Basin. It was characterised by abundant Quadrisporites horridus in association with Endosporites radiatus, ProtohapZoxypinus spp. and StriomonoscLOcites with minor proportions of species which characterised the underlying Dulhuntyispova Assem blage. This assemblage is possibly best compared with

Hennelly's "transition zone" microflora (1958) and Helby's - 27-

(in Packhara, 1969) lowermost Narrabeen Group microflora.

The succeeding Unit Tr lb was marked by the first appearance of Lunatispovites in association with Falod- sporites and a number of undescribed pteridophytic forms.

Evans implied a corystospermaceous affinity for the

Faloispordtes pollen, although current knowledge of the distribution of these plants may suggest otherwise. Unit

Tr lb was recognised in the Bowen Basin and Eromanga Basin but was not recognised at that time in the Sydney Basin, although the author speculated on its widespread occurrence.

The base of Unit Tr 2a was marked by a significant decline in the prominence of the large gymnospermous pollen.

Lunatdspordtes was reported as the most prominent bisaccate form and was associated with Lundbtaddspora which made its first appearance in this assemblage. The unit was reported from the Collaroy Claystone of the Sydney Basin

(see stratigraphic section), the upper portion of the Rewan

Formation in the Bowen Basin and was widely developed in the Eromanga Basin. Evans equated this unit with the microflora of the Kockatea Shale, cautiously acknowledging the implication of a Permian age for the lower units. Unit

Tr2b was characterised by the first appearance of Aratrds- porites and the last occurrence of Lundbladispora. Falcis- pordtes becomes increasingly prominent throughout the assemblage. Evans reported this assemblage from the upper most portion of the Rewan Formation (see also de Jersey

1968, figure 3) in the Bowen Basin and close to the top of the Collaroy Claystone in the Sydney Basin. - 28-

Unit Tr3 is characterised by an abundance of

FaZoisporites which Evans related to the increased

corystosperm content of the Dioroidium flora. Four

assemblages have been delineated within Unit Tr3. Evans

suggested that the lower two assemblages, Tr 3a and Tr 3b,

occupied the Gosford Formation, Hawkesbury Sandstone and

the Wianamatta Group in the Sydney Basin and extended from

uppermost Rewan Formation to basal Moolayember Formation

in the Bowen Basin. These units were distinguished by the

appearance of Aratrisporites fiseheri (see description of

A. parvispinosus) in unit Tr 3b. It was suggested that

Aratrisporites does not extend beyond Unit Tr 3b. The

upper two units, Tr 3c and Tr 3d were distinguished by

the absence of Aratrisporites 3 the appearance of DupZexi-

sporites gyratus delineating the base of Unit Tr 3d. Unit

Tr 3d was stated to occupy the Ipswich Coal Measures and

the Bundamba Group of the Ipswich-Clarence Basin. The validity of the concept of mutual exclusion of Aratrisporites

and Duplexisporites gyratus 3 on which the division of Units

Tr 3b, Tr 3c and Tr 3d is based is no longer acceptable.

Playford & Dettmann (1965) report these forms from the

same Leigh Creek assemblages, Hill et at. (1965) report

Aratrisporites from the Blackstone Formation (Evans Tr 3c)

of the Ipswich Coal Measures. These forms also occur

together in the Moolayember Formation (de Jersey & Hamilton,

1967), the Hawkesbury Sandstone and Wianamatta Group (Helby

in Packham, 1969) and in the Wandoan Formation (de Jersey &

Hamilton, 1969). COMPARATIVE RANGES

OF SOME

AUSTRALIAN LATE PERMIAN - TRIASSIC MICROFLORAS

Falcisporiles spp.

Lunalisporiles spp.

Aratrisporiles spp Aratrisporiles panAspinosus Cadargasporites senectus Circulina sp.

Classopollis sp.

de Jersey ( 1949)

Toy lor ( 1953 )

Hennelly ( 1 959)

Dettomann ( 1961 )

de Jersey ( 1962 )

Helby ( 1962)

Balme ( 1963 )

Playford & Dettmann ( 1 955)

Playford ( 1965 )

de Jersey & Hamilton (1965a)

de Jersey & Hamilton (1965b)

Helby ( 1967 )

de Jersey & Hamilton ( 1 957)

de Jersey ( 1968 )

Helby (in Packham, 1970)

Evans ( 1966 )

PERMIAN TRIASSIC JURASSIC

FIGURE 3 - 29 -

A biostratigraphic synthesis of the data reviewed above

is presented on Figure 3.

OBSERVATIONS

2.Í. STRATIGRAPHY

A comprehensive discussion of the stratigraphy of the

Permian and Triassic rocks associated with the Sydney Basin is

presented in Packham (1969). Table 1 (below) summarises the

nomenclatural stratigraphy of regional sequences and is adapted

from Packham (1969,, Tables 5.1, 5.2, 5.32 and 7.1). In this

study I am principally concerned with sections above the horizon

represented by the thickened line on Table 1. This line is

usually drawn at the top of the coal measure sequence and is

commonly regarded as the location of the Permian-Triassic bound

ary. Balme (1969) and Helby (in Packham 1969) indicate that

this horizon is actually located within the Late Permian.

TABLE 1 PERMIAN - TRIASSIC SEQUENCES ASSOCIATED WITH THE SYDNEY BASIN

CENTRAL AND LOWER HUNTER SINGLETON - BAERAM I - U L A N WILLOWTREE DUBBO-COBBORAH DUNEDOO-BINNAWAY SOUTH COAST VALLEY MUSWELLBROOK

Wionomotto Group Napp«rby Beds

Lower Lower

Howkesbury Sondston« Bal I ¡mor« Merrygoen

Beds Beds

Narroboen Group Narrob««n Group Narrobeen Group Digby Beds

Newcostle lllawarra Cool Measures Cool Measures Singleton Block Jock Undifferentiated lllawarra Coal Measures Undifferentiated Permian Cool Measures Coal Measures Perm ion Tomogo Cool Measures

•?----- ? ----- ?-----? ----- ? ----- ? ----- ? ----- ? ----- 0-

Shoal haven Group Gladstone Formation Toll Bor Group Shoolhaven Group Maitland Group

Bor ambi I Crook Greta Cool Measures Porcupine Formation Formation

Willow Tree Nandewar Group Coal Measures Dal wood Group Gyrran Volcanics

Clyde Cool Measures I Volcanics

- 30-

The Late Permian-Triassic sequence of the Sydney Basin

can be arranged into two broad lithostratigraphic provinces.

The southern province which is arbitrarily delineated from the

northern province along the Goulburn River is characterised by

the outcrops extending from the coast to the Blue Mountains and

constitutes three major rock units. These are, in ascending

order, the Narrabeen Group, the Hawkesbury Sandstone and the

Wianamatta Group.

The Narrabeen Group.

The Narrabeen . Group (Hanlon e~t clZ . 3 1954) is composed

principally of deltaic and fluvial sediments. Intercalations

of red—green siltstones and claystones are increasingly pro

minent towards the north.

Figure 2 shows that the Narrabeen Group attains a maximum

thickness in excess of 2,300 ft. in the vicinity of the Hawkes

bury River. The section thins gradually to the vicinity of

Sydney, south of which thinning is more rapid. Similarly,

TABLE 2 NARRABEEN GROUP STRATIGRAPHY - SOUTH COAST

Average h a w k e s b u r y s a n d s t o n e 0UARTZOSE SANDSTONE Outcrop Thickness

Newport For motion 0 » n sillslone and shale *»ith quarit-lithic sandstones Shales contain well preserved 35 ft. ( formerly Got lord F or mot i on ) plant assemblages

Bold Hill Cloyttone Red-brown cla\ stones and siltstones mi th occasional lithic sandstone lenses. 50 ft.

( includes Gone Member at top) Heddtng not preserved

l»ane Member consists of kaolinilic pellet clay stone ( " lo n s le in " ).

fi. i Bulpo Sandstone Lithic and ijuartr-lithic sandstones siltstones and occasional shales. 390 ft. 1 Red clay stone partings appear in upper part of section. i 5 Stonwell Porb C loy stone Red-brown to green claystones and siltstones with thin fine grained lithic sandstones. 130 ft. ■ *< * % I Sc arbor ©ufh Sandstone Grey-green lithic and quarti—lithic sandstone and conglomerate. a s It.

3 Wombarra Shale Mainly grey-green sillstone. with some grey shale. Plant debns often abundant 130 ft. 1 ( includes Otford Sandstone Msmbsr) on bedding planes. Otford Sandstone Member comprised of grey-green lithic sandstone.

Coolcliff Sondstone Grey, medium grained lithic sandstone with pebbly bands. » f t .

M 1 AWAWWO S v lli Sm m Coal. GOAL MEASURES - 31- the section thins gradually to the west, the rate of thinning becoming more pronounced approaching the western limit of out crop (Bradley 1964 - unpublished). A compilation of the various detailed studies of the Sydney Basin is given by McElroy {in

Packham, 1969). These studies have been concentrated in three main areas due to the nature of outcrop.

The most celebrated Narrabeen Group section occurs along the coastal outcrop between Garie Beach and Wollongong. Seven rock units have been delineated within this section by Hanlon et at. (1954). Details of the section are presented in Table 2.

These formations maintain their identity in the immediate vicinity of the coastal section. However, Brunker {in Packham,

1969) reports steadily increasing sand content to the west, particularly at the horizons of the Wombarra Shale and Stanwell

Park Claystone. Hanlon et at. (1954, p . 117) indicate that ‘the base of the Narrabeen Group in the Scarborough-Clifton area is drawn immediately above the Bulli Seam. This definition is generally applied throughout the southern coalfield.

Partial sections of the Narrabeen Group crop out almost continuously along the coast between Long Reef and Swansea to the north of Sydney. Based on a synthesis of outcrop and sub surface data Hanlon et at. (1954) delineated four formations.

The major features of these units are outlined on Table 3. These authors placed the base of the Narrabeen Group immediately above the Wallarah Seam of the Newcastle Coal Measures. However, recent drilling has revealed additional coal measure sedimen tation in the vicinity of Lake Munmorah. This additional section, - 32-

t a b l e 3 NARRABEEN GROUP STRATIGRAPHY - LONG REEF TO SWANSEA

h a w k e s b u r y s a n d s t o n e QUARTZOSE SANDSTONE Tkicknotis

Go »lord Sub-Group Grey siltstones and shales with quartz and quartz-lithic sandstones. Certain shales 800 ft. (Form erly Go »ford For motion ) and silts contain well preserved plant assemblages Single red—brown clay stone ( Inc ludo • Now port For mot ion of top) horizon reported from central portion of the formation.

PATONGA CLAYSTONE Red-brown siltstones and claysiones with occasional grey shale and fine lithic sandstone interbeds. Green silts tone and clay stone interbeds towards base of the formation.

£ TUGGERAH FORMATION Red-brown and green siltstones and claysiones interbedded with quartz-lithic sandstones < r and conglomerates. i a MUNMORAH CONGLOMERATE Quartz-lithic pebbly sandstones, with massive conglomerate lenses. Green siltstones with mottled red phases relatively common. Occasional grey siltstones and shales in lower position

VoIm Point Cool Mo mb or Karignon Cong lomo roto Mombor Wallarah Tuff Mombor

VALLARAN SEAM

which includes the Wallarah Tuff Member, the Karignan Conglomerate

Member and the Vales Point Coal Member, has been discussed by

McKenzie and Britten (in Packham, 1969). These authors suggest

that the lithology of the Karignan Conglomerate Member is

closely similar to the Taralba Conglomerate and similar older units. They indicate that the basal portion of the Munmorah

Conglomerate is characterised by finer, more angular pebbles and has a more quartzose matrix than the conglomerates below the

Vales Point Coal Member. Finer sediments occurring between the

Wallarah Seam and the Vales Point Coal Member are crowded with

Glossopteris. The complete dominance of the Glossopteris flora is also reflected in microfloras recovered from this section

(discussed below). Despite the closer similarity of the sedi ments in this additional section to the underlying Newcastle

Coal Measures, all previous authors including Engel (1966) and

McKenzie & Britten (in Fackhani, 1969) refer this section to the

Narrabeen Group. In the interests of nomenclatural and concept - 33- uniformity I believe this section should be assigned to the

Newcastle Coal Measures.

A considerable contribution to the understanding of the

Narrabeen Group was made by Bradley (1964 - unpublished), who produced a number of graphic interpretations of Narrabeen Group sections, compiled from sub-surface data. These sections illu strate a number of misinterpretations in the stratigraphic synthesis of the Wyong - Narrabeen area by Hanlon et al. (1954).

These authors assumed that the "chocolate claystones" cropping out in the vicinity of Collaroy were continuous with similar sediments encountered in Windeyer's Hawkesbury River

Bore between 776 ft. and 1,224 ft. 6 ins. Figure 2, which is adapted from Bradley (1964), clearly shows that the Collaroy outcrop is continuous with the Bald Hill Claystone. However, this horizon is considerably higher than the sequence in

Windeyer's Hawkesbury River Bore which Hanlon et al. (1954) designated as type section of the Collaroy Claystone. McElroy

{in Packham, 1969) has suggested that the lower claystone unit including the type section of the Collaroy Claystone be renamed the Patonga Claystone. This suggestion is tentatively followed, although it may contravene paragrah 36 of the Australian Code of

Stratigraphic Nomenclature (1964). Stuntz (in press) raises the

Gosford Formation to Sub-group status, and proposes that the section between the Bald Hill Claystone and the Hawkesbury

Sandstone be named the Newport Formation. A detailed discussion of this section is presented by Branagan, Packham & Webby (1966). - 34-

The vertical cliffs which characterise the scenery of the

deeply dissected Blue Mountains Plateau to the west of Sydney

are composed predominantly of Narrabeen Group sediments. The valley systems of the Blue Mountains reveal many almost complete

sections which are continuous over relatively long distances.

The first detailed study within the area was that of Crook (1957),

in which three distinct lithostratigraphic units were delineated

in the Grose Valley (see Table 4). These are, in ascending order,

TABLE 4 NARRABEEN GROUP STRATIGRAPHY - BLUE MOUNTAINS AREA

the Caley Formation, the Grose Sandstone and the Burralow Form ation. Crook's division of the Narrabeen Group was extended to the Burragorang area by Helby (1961 - unpublished, summary in

Packham, 1969). Helby delineated five informal members in the

Caley Formation throughout the Burragorang area. He also recog nised two distinct sandstone members, separated by a relatively thick claystone horizon, in the Grose Sandstone. Independently, -35

Goldbery (1966 - unpublished) recognised a similar sub-division

to the north and extended this into the type area. These sub divisions have been formalised by Goldbery (in press) and are

shown on Table 4. Recent unpublished studies by T. Dickson and R. Goldbery of the New South Wales Geological Survey indi cate that members of the Caley Formation are continuous for at least 60 miles along depositional strike.

A synthesis of Narrabeen Group correlations between the areas discussed above has been presented by McElroy (Table 5.16 in Packham, 1969). These correlations which were adapted from

Hanlon et at. (1954) and Crook (1957) are reproduced on Table 5.

TABLE 5 SUBDIVISIONS OF THE NARRABEEN GROUP SHOWING CORRELATION BETWEEN THE NARRABEEN - WYONG, SOUTH COAST AND COLO - GROSE DISTRICTS WITH THICKNESS IN TYPE SECTIONS.

Reproduced from McElroy Table 5 16 (in Packham, 1969).

r Narrabeen - Wyong ond Norrobeen - Wyong District South Coast District South Coast Districts Colo - Grose Districts Former Nomonclature

Mongrove Sandstone Member)

Gosford Formation Ourimboh Sandstone Member) No members named Upper Stage

Wyong Sandstone Member )

Burralow Formation

Bald Hill Claystone - Tabarag Sandstone Member Collaroy Claystone Middle Stage

Bulgo Sandstone Grose Sandstone

Tuggeroh Formation Stanwell Pork Claystone

C lif t o n Scarborough Sandstone

S u b - G r o u p Womborro Shale Munmorah Conglomerate Caley Formation Lower Stage — Otford Sandstone Member

Coal Cliff Sandstone

Newcastle Coal Measure. lllawarra Coal Measures lllawarro Cool Measures

The correlations on Table 5 perpetuate misinterpretations of Hanlon et at. discussed above. They also suggest equivalence of the Caley Formation, Munmorah Conglomerate and the interval - 36- occupied by the Coalcliff Sandstone, Wombarra Shale and Scar borough Sandstone on the south coast. Helby (1961, Table 4,4)

suggested that the Caley Formation was equivalent to the interval on the south Coast section occupied by the Coalcliff Sandstone and Wombarra Shale. Independently Bradley (1964), Dickson

Cpers. comm.) and Golbery (1966) have proposed a similar cor relation. Table 6 represents a synthesis of correlations of the Narrabeen Group, based on these more recent studies.

TABLE 6 SUGGESTED CORRELATIONS OF NARRABEEN GROUP SEQUENCES

SOUTH COAST DISTRICT BLUE MOUNTAINS PLATEAU LONG REEF TO SWANSEA

| l _ Newport Formation Newport Formation , o §

Burralow Formation j j * ? |

Bold Hill Claystone Bald Hill Claystone? k I J S Í » & w

Bulgo Sandstone Patanga Claystone

1 Grose Sandstone 3 Stonwell Park Clay stone Tuggerah Formation 1 8

Scarborough Sond stone

Wombarra Shale Munmorah Conglomerate

Caley Formation

CoaicliW Sandstone

The fossil lists assembled by Raggatt (in Packham, 1969) represent the only published synthesis of the biostratigraphy of the Narrabeen Group. Although extensive and diverse floras - 37- are known from sections best assigned to the Gosford Sub-Group, published data concerning the floral assemblages of the lower part of the Narrabeen Group are both rare and fragmentary. The extension of many elements of the Glossopteris flora into the lowermost portion of the Narrabeen Group is well established.

Collections from this part of the section have been described by Dun (1910, 1911) and Walkom (1925). Raggatt (in Packham,

1969) lists many of the forms reported by earlier workers.

Recent collections suggest that a form tentatively identified as ?Thinnfeldia callipteroid.es Carpentier (identified by Dr.

J.A. Townrow), may be stratigraphica1ly significant. This species is locally dominant and is a constant component of the lowermost Narrabeen Group floral assemblages.

Plant remains are not normally abundant in sections equi valent to the Tuggerah Formation and the Patonga Claystone.

Raggatt (in Packham, 1969) reports Schizoneura^ ?Sagenopteris3

?Alethopteris3 ZeugophyHites> Phyllotheca and Dicroidium narrabeenensis from this part of the sequence. The lowest authenticated occurrence of Dicroidium odontopteroides is at 828 feet (lower portion of Tuggerah Formation) in Ourimbah

Creek D.D.H. No. 5 (see descriptions of samples 566 and 567).

All occurrences of this form appear to be confined to inter calations of grey-green sandy siltstone. The grey shales, which are most intimately associated with the red beds contain frag mented PhyZ'lotheca and occasional coniferous remains.

The flora of the Gosford Sub-Group is largely dominated by Dicroidium and Hoegia. Abundant and diverse plant assem blages occur throughout the section, usually associated with - 38 - sediments which are readily identified as being deposited in delta plain (backswamp) and lacustrine environments. The major elements of this flora have been described by Walkom (1925) and

Burges (1935).

Actual vertebrate remains in the Narrabeen Group are reported from a single locality at Gosford. This horizon occurs within the Gosford Sub-Group, although its precise location in the section is yet to be determined. The fauna includes a diverse fish assemblage including members of five osteichthyan families. The assemblage was described by Woodward (1890), who suggested a Keuper (Late Triassic) age. Stephens (1887) described Blinasaurus (Platyeeps) witkon&orli from this locality.

Parotosaurus wadei is also reported from this assemblage by

Cosgriff (1967). Based on a study of the comparative development of the otic area of P. wadei3 Cosgriff suggests a lower Triassic age for the Gosford vertebrate assemblage. Vertebrate footprints occur on the rock platform at Turrimetta Headland, close to the base of the Newport Formation. Footprints are also relatively common in the Coalcliff Sandstone, where they have been tenta tively identified as cf. Iehnium gampsodaetylum (Harper, 1915).

Although completely overshadowed by the more attractive vertebrate remains, a sparse invertebrate fauna occurs throughout

Narrabeen Group sediments. Foraminifera including Ammobaculites3

Haplophragmiumj cf. Troehammina and cf. Verneuilina have been reported by Crespin (1938 - unpublished) from the Kulnura Bore.

However, it has not been possible to relocate this material in the collections of the Bureau of Mineral Resources. These forms occur in association with fish scales and siliceous sponge - 39-

spicules at an equivalent horizon to the Tuggerah Formation.

This would appear to correspond to an acritarch horizon

encountered in Terrigal D.D.H. No.l (Dr. P.R. Evans,pers. comm.). Conolly (1969) reports unidentified ostracods and foraminifera from thin sections of the Bald Hill Claystone.

Coralline algae are also relatively common in the upper portion of the Bald Hill Claystone at Avalon (G.H. Packham, pers. comm.).

Pelecypods, although not abundant, have been found with increasing regularity in the upper portion of the Gosford

Sub-Group. I have also encountered small, undescribed pelecypods in the Coalcliff Sandstone (Sample 437) in the Camden D.D.H. No.61.

Cyzicus is locally prominent throughout the section below the base of the Gosford Sub-Group. However, it is noted that it has not been reported in association with the "red beds".

Traditionally the boundary of the Permian and Triassic

Systems in the Sydney Basin is drawn at the top of the respective coal measure sequences (see Table 1). Present lithostratigraphic data suggest that these surfaces are diachronous, although not necessarily the result of an extensive erosional hiatus. In the apparent absence of reliable marine invertebrates the decline of the Gtossopteris flora, which is considered coincident with the cessation of coal measure sedimentation, is usually regarded as marking the boundary. However, there is some doubt concerning the validity of this concept. As indicated above (p.37) the extension of the Glos sopter-is flora into the Narrabeen Group and its equivalents is well established. Despite the appearance of a number of new plant forms Walkom (1925) suggests that the basal

Narrabeen Group assemblage "..... is obviously more closely - 40 -

re la t ed to the Permian flora than to the typical Mesozoic

flora." It should be noted that the first authenticated

Dieroidium is reported from the Tuggerah Formation (see page 57 ) and is more or less coincident with the last reported occurrence of Schizoneura (Raggatt, 1938).

The decline and replacement of the Glos sopteris flora is most vividly illustrated by the microfloral sequence. Hennelly

(1938) recognised and described the abrupt change from the

Dulhuntyispora assemblage of the coal measures (Balme, 1964) to a new basal Narrabeen Group microflora. Although containing a number of elements characteristic of the Dulhuntyispora assemblage this new microflora was dominated by Falcisporites

("Pityosporites”)nigraoristatus and Protohaploxypinus

("P'ityospor'ites")reticulatus together with a number of dis tinctive pteridophytic forms. Hennelly interpreted the basal two feet of the sequence in Appin D.D.H. No. 4 as representing a Permian-Triassic transition zone. Evans (1963) subscribed to Hennelly's interpretation in assigning the basal portion of the Rewan Formation of the Bowen Basin to the Early Triassic.

Helby (1962 - unpublished) recognised two microfloral assemblages associated with the Grose Sandstone in the Burra- gorang area. The lower assemblage was compared to western

European and Canadian Late Permian microfloras while the upper assemblage was correlated with the microflora of the Early

Triassic Kockatea Shale of Western Australia. Balme (1963) established the " Taeniaesporites" microflora of the Kockatea

Shale as basal Triassic. It was concluded that the lower por tion of the Narrabeen Group, including most of the lower member - 41-

of the Grose Sandstone, should be assigned to the Permian

System. Evans (1966) confirmed this correlation with the

Kockatea Shale microflora, briefly discussing the implications.

Helby {in Packham, 1969) reviewed the more recent palynological

data concerning the boundary in other Gondwana localities and

suggested that the boundary of the Permian and Triassic Systems

in the Narrabeen Group should be located close to the base of

the " Taeniaesporites" microflora. This microflora was stated

as first appearing in the Scarborough Sandstone, the upper

portion of the Caley Formation and the central portion of the

Munmorah Conglomerate.

In a comprehensive review of all available data concerning

the Permian-Triassic Boundary in Australia Balme (1969) con

cluded that the base of the "Taeniaesporites" microflora was

presently the most appropriate location for the boundary.

The Hawkesbury Sandstone.

The Hawkesbury Sandstone is essentially a medium to coarse, well sorted quartz sand, and attains a maximum thickness of

about 950 feet (Galloway, 1968). Individual beds often appear massive, ranging in thickness from less than 1 ft. to 50 ft.

These beds are usually lenticular and often characterised by

large scale, steeply dipping cross laminations. In most

localities the Hawkesbury Sandstone conformably overlies the

Gosford Sub-Group and its equivalents. However, erosional breaks are often evident. To the extreme south-west the

Hawkesbury Sandstone may overlap the entire Narrabeen Group

(Standard in Packham, 1969) although Dickson (1969) suggests - 42- that the two units are indistinguishable in the Sutton Forest area.

The lenticular nature of the beds constituting the

Hawkesbury Sandstone has hindered detailed stratigraphic analyses. It is, however, generally accepted that the pro portion of siltstone and possibly shale increases towards the top of the formation. Branagan (1969) and Standard (1961) have indicated that thick siltstone intercalations are more prominent to the north of the Hawkesbury River. Thin claystone bands are more commonly encountered in the lower parts of the section. Branagan (1969) also suggests that two significant horizons of contorted sediments can be recognised in the Sydney ar ea .

The most exhaustive study of the Hawkesbury Sandstone, to date, is that of Standard (1964 - unpublished). A summary of this work is presented by Standard (in Packham, 1969).

Despite the apparent uniformity of composition and sedimentary style, this formation remains the least understood and perhaps most controversial rock unit in the Sydney Basin. The main points of contention include the areal distribution of the formation, its composition and the environment of deposition.

The areal distribution of the Hawkesbury Sandstone is usually questioned becaused of the difficulty in delineating this unit from parts of the underlying Gosford Sub-Group and its equi valents. Though the latter unit is composed essentially of quartz lithie sands interbedded with silts in the vicinity of - 43 -

the present coastline, quartz is an increasingly prominent

component towards the west. Crook (1957, Table 1) reports

sands from the Burralow Formation with quartz content in excess

of 88%. Standard (1961, p.145) outlined a number of criteria

for delineating these units and subsequently (Standard, 1964)

considerably restricted the area of Hawkesbury Sandstone out

crop. This work of Standard, although generally accepted has

been substantially modified by Galloway (1968) and Goldbery (1969).

Standard {in Packham, 1969) indicates that the average modal

analysis of the Hawkesbury Sandstone would display a detrital

quartz component of 68% and a clay matrix content of 20%. These

figures are at variance with those of Crook (1957), Golding

(1959), Helby (1961) and McElroy (1954). They are also difficult

to reconcile with observations made by J.R. Conolly (pers. comm.) and G.H. Packham {pers. comm.) These other workers are unanimous

in indicating a substantially higher quartz content and lower proportion of clay matrix.

The apparent absence of obvious marine fossils has fostered

the concept of a non-marine environment of deposition for the

Hawkesbury Sandstone. Based on analysis of detailed measurements of cross laminations of the unit, Standard {in Packham, 1969) has suggested that the sediments were deposited by a fluvial system originating in the far south-west. Branagan {ibid.) suggests that the environment was fluvio-deltaic. Both these hypotheses fail to account for the almost complete absence of

inter-related sedimentary features such as levee, back swamp and delta plain deposits, point bar systems and channel sands. - 44-

Conolly (1969) has tentatively suggested that the Hawkesbury Sandstone can be compared with modern tidal delta-barrier

bar systems. Goldbery (1969 - unpublished) also envisages a barrier bar origin for the unit.

Knowledge of the fauna and flora of the Hawkesbury Sand

stone is almost confined to occurrences in siltstone layers,

which are concentrated towards the top of the formation. An abundant fish fauna, including representatives of nine ostei-

chthyan families has been described from Brookvale, near Sydney

by Wade (1935). Similar but more restricted faunas have been

reported from Tambourine Bay, North Turramurra and Asquith.

Wade (1935, p.86) suggests a "Mid-Middle Triassic" age for

the Brookvale occurrences. Parotosaurus (Suboyclotosaurus) brookvalensis3 a capitosaur from the Brookvale Quarry is interpreted by Cosgriff (1967) as representing an intermediate evolutionary position between P. wadei and Paraoyolotosaurus davidi. Cosgriff suggests an Early Triassic age for P. wadei (Gosford Sub-Group) and a Mid to Late Triassic age for P. davidi (Ashfield Shale). A thoracic plate, tentatively assigned to Mastodonosaurus platyceps is reported from the Cockatoo Dock excavation. Sherwin (1969) discusses the occurrence of verte brate footprints in the upper part of the formation. He suggests

that they can be related to Stereospondy1 amphibians. Elements

of an insect assemblage collected at Brookvale Quarry have been

described by McKeown (1937) and Tillyard (1925). Rare occur

rences of Unio and Cyzi-cus are recorded in David (1950).

Standard (1964 - unpublished) reports a small unidentified - 45- gastropod from Mt. Yengo. Etheridge jnr. (1888) describes a

bellerophont gastropod Tremanotus maideni collected from

excavation of docks in Sydney Harbour. These gastropods

are usually regarded as marine animals and supposedly became

extinct during the Early Triassic.

Plant remains are common in most siltstone bands throughout

the formation. However, apart from the occurrences at Brookvale,

comprehensive collections are not available. A list of prominent forms is presented by Branagan {in Packham, 1969).

The Wianamatta Group. The Wianamatta Group outcrops over a large portion of the

Cumberland Plain with occasional outliers on higher ridges of the adjacent plateau system. The group is composed of alter nating units of shaley siltstones and lithic sandstones. It conformably overlies the Hawkesbury Sandstone and apart from a few modified remnants below ? Tertiary basalt (Mt. Yengo, etc.) the upper portion of the sequence is confined to the vicinity of the Razorback Range.

The most comprehensive study of the Wianamatta Group is

that of Lovering (1954). Lovering divided the sequence into two sub-groups, along the lines suggested by Browne {in David,

1950). The lower Liverpool Sub-Group was characterised by a predominantly shale sequence, whilst the upper Camden Sub-Group contained a more prominent sandstone component. The sequence was further sub-divided into nine formations. The essential features of these units are set out on Table 6. Lovering named three formations from the Liverpool Sub-Group. These were, in - 46 - ascending order, the Ashfield Shale, the Minchinbury Sandstone and the Bringelly Shale. Recent work by Herbert has considerably modified Lovering's Liverpool Sub-Group divisions. McElroy

(in Packham, 1969) has delineated a formation, the Mittagong

Formation, which is transitional between the Hawkesbury Sand

stone and the Ashfield Shale. This unit, which has previously been referred to as the "Passage Beds", is not as extensive as

the overlying Ashfield Shale.

Herbert (in press) has demonstrated that the Minchinbury

Sandstone of Lovering comprises a number of discrete sand bodies occurring on at least three stratigraphic horizons. In

accordance with the Australian Code of Stratigraphic Nomen

clature (1964) he interprets these bodies as members of the

Bringelly Shale. He further illustrates a major lithological

break within the Ashfield Shale of Lovering (1954). The lower

TABLE 7

STRATIGRAPHY OF THE WIANAMATTA GROUP

Ah»r Lov.rtng 1954 Aftor Horbort ( in prats ) Avorogo Thickmoss

Prudhoo Shalo Siltslone and shale with interbeds of lithic and calcareous sandstone. 170 It.

3 Picton Formation Alternating lithic sandstones, siltsiones and shales. 100 ft. i

R a z o r bock S a n d s ton« Massive lithic sandstones with occasional shale partings. 70 f t . DEN S ilt

3 A n n a n Sh o t« Dark brown siltsiones and shales, with occasional lithic sandstone lenses. 40 f t .

P o tt« H ill S a n d s ton« Lithic and calcareous sandstone 40 f t . fc

ft. 2 Bringolly Shalo Dark grey to brown siltsiones interbedded with lithic and calcareous sandstones. 1 Bringolly Shalo 4 00 ft. Occasional carbonaceous shale and coal horizons encountered.

SUB M inchinbury Sands ton«

3 1 Ashfiald Shalo Black carbonaceous siltsiones and shales, often sideritic, occasional coal horizons. 100 f t . A*M:.M 5hal.

3 Mittogong Formation Alternating black siltsiones and fine quartgose sandstone. 0 - 5 0 ft.

Howkoobury Sands ton« - 47- portion of the Ashfield Shale, as defined by Lovering, is composed of carbonaceous siltstones and shales often intensely sideritic. There are occasional interbeds of quartzose sand stone, similar in lithology to the underlying Hawkesbury Sand stone. The upper portion consists predominantly of grey to brown siltstone and is distinguishable from the overlying

Bringelly Shale. Herbert restricts the Ashfield Shale to the section comprised of black, sideritic and carbonaceous siltstones and shales. The Bringelly Shale is extended to include the remainder of the sequence. The coarser fractions of the

Bringelly Shale are distinctly lithic and usually glauconitic.

Herbert indicates they may contain up to 70% rounded volcanic rock fragments. Recent work by Hamilton, Helby and Taylor

(in press) indicates a correlation between this change of lithology in the Liverpool Sub-Group and the advent of con temporaneous volcanic activity in the immediate vicinity.

The environment of deposition of the Wianamatta Group is discussed by Lovering (1954), Conolly (1969) and Herbert

(in press). There is general agreement that the conditions during deposition of the Mittagong Formation and the Ashfield

Shale fluctuated between a brackish, possibly tidal marsh environment to conditions essentially similar to those existing during deposition of the Hawkesbury Sandstone. Conolly has suggested that deposition in these environments was probably contemporaneous. The environment of deposition of sediments in the sequence above Ashfield Shale is fairly uniform. It is generally interpreted as an estuarine, tidal-flat system inter- - 48-

mittently covered by regressive fluvio-deltaic developments.

A review of the fossil occurrences of the Wianamatta Group

is included in Lovering (1954). Apart from a microfauna com

prising foraminifera and ostracods in the Minchinbury Sandstone

known faunal occurrences are presently restricted to the

Mittagong Formation and Ashfield Shale. Chapman (1909)

described this microfauna, indicating that it included a

number of "Rhaetic and Lower Jurassic types". However,

Lovering (1953) expresses some doubts concerning Chapman’s

identifications and the reliability of the Jurassic age

assigned to the fauna. A restricted pelecypod assemblage

occurs intermittently throughout the Mittagong Formation

and into the basal portion of the Ashfield Shale. Tillyard

(1916) described a number of insects from the Ashfield Shale

at the St. Peters Quarry.

The vertebrate fauna occurring in the lower portion of the

Liverpool Sub-Group is considerably more diverse than the

invertebrates. An extensive fish fauna is reported from the

Ashfield Shale sequence in the St. Peters Brickpit. The fauna

consists of thirteen species which occur in two distinct

assemblages (Woodward 1908). The significance of these

assemblages has not been established. Elements of the fauna have been encountered throughout the Sydney district. An

extremely abundant assemblage is also known from Bowral

(Dr. A. Howie, pers. comm.) A number of amphibians are also known from the lower portion of the Ashfield Shale. These

include Paracyclotosaurus davidi3 Notobrachyops picketti and - 49- capitosaurid remains from the Bowral area which have been referred previously to Mastodonosaurus (see David 1950, p.431).

Cosgriff (1967) suggests that the development of the otic region of Paraoyolotosaurus davidi indicates a Mid or Late

Trias sic age.

Although Phyitotheoa fragments and plant debris are relatively abundant in all formations of the Wianamatta Group distinct plant assemblages are seldom encountered (see Lovering

1954). However, the existence of a relatively diverse and abundant flora is suggested by the microflora of the Wianamatta

Group (Helby in Packham, 1969). The presence of an abundant flora in more fluviatile environments is also indicated by a number of cuticle rich coals in the Liverpool Sub-Group.

Northern province of the Sydney Basin.

The sediments which characterise the northern province crop out extensively along the eastern and south-eastern margins of the Coonamble Lobe of the Great Australian Basin.

They are also recognised from subsurface data provided by water bores and oil exploration drilling. The western limits of this sequence below the Jurassic cover are uncertain. The sequence is composed principally of fluviatile and lacustrine sediments. However, intercalations of red and green siltstones and claystones are increasingly prominent to the extreme south east where the lower part of the sequence merges with the lower portion of the Narrabeen Group.

Early stratigraphic studies of Late Permian-Triassic sequences along the margin of the Coonamble Lobe include - 50- work by Kenny (1926, 1929, 1963), Kenny & Mulholland (1928),

Lloyd (1935) and Dulhunty (1938, 1939a, b, 1940). These early investigations were concerned with extremely local sections resulting in a confused multiplicity of stratigraphic nomen clature. An attempted 1ithostratigraphic correlation of some of these sequences is illustrated on Table 1.

Despite the confusion of nomenclature a common sedimentary sequence can be recognised throughout the area. It consists of a basal conglomeratic unit with prominent horizons of red and green siltstone at the base, overlain by a thick, massive sandy unit which is in turn overlain by a series of flaggy sandstones interbedded with brown to dark grey carbonaceous shales and silt stones.

The lowest unit in the sequence is composed essentially of pebbly sandstone. Irregular bodies of green and red siltstone and claystones occur at the base of the section along the Goulburn River. These are interbedded with conglomerate lenses and pass up into conglomeratic sandstones. The unit conformably overlies the Late Permian coal measures (?Illawarra

Coal Measures). However, erosional breaks are usually evident and the coal measures are overlapped on the edges of a number of basement features to the west. The basal conglomerates are characterised by red and green jasper and a wide assortment of igneous and metasediment pebbles. Maximum development of the unit occurs along the eastern edge of the Great Artesian

Basin (about 500 feet) immediately to the north of the Liverpool

Range, adjacent to the western edge of the Carboniferous rocks of the New England Fold Belt. It would appear that the con- - 51- glomerates are largely derived from the fold belt to the east.

The unit thins gradually to the west where it has been recognised along the southern margin of the Great Artesian Basin (Dulhunty

1938, 1939a, b, 1940), a much thinner extension being recog nised in water bores between Dunedoo and Dubbo. It also thins rapidly to the north-west where it has been recognised by Kenny

(1929) in the Gunnedah area and in the vicinity of Boggabri by Hanlon (1950 a, b). It appears to thicken to the south-east, merging with the lower portion of the Narrabeen Group. Micro floras recovered from claystone bands within this facies indicate that the upper limit of the unit is diachronous.

The conglomerate unit passes up into a thick sandy unit, composed of massive quartoze sandstones and siltstones. Several thick chocolate claystone horizons occur in the lower portion.

Clay shales become common towards the top of the section. The unit has a maximum recorded thickness of about 700 feet - on the western edge of the Goulburn River Valley, thinning markedly to the north-west. Its precise relationship with the sequence to the south-east has not been established. This sandy unit, together with the underlying conglomeratic unit are represented in the Gunnedah area by the Digby Beds, the Binnaway area by at least the basal lower Merrygoen Beds (possibly the larger portion of the lower Merrygoen Beds) and in the Dubbo district by the greater portion of the lower Ballimore Beds. They are also represented along the Goulburn River valley by part of the Wollar Sandstone.

The middle sandy unit of the Triassic sequence, is overlain by a section of flaggy sandstones, interbedded with brown - 52- to dark grey, carbonaceous siltstones and shales. Kenny

(1929) reports a maximum thickness (700 feet) for the Napperby

Beds in the Gunnedah-Coonabarabran district. From the des cription of the sediments they appear to be identifiable as this upper unit. Thickness of the unit along the southern margin of the Coonamble Lobe ranges from 45-150 feet. The unit appears to be represented in Bohena No. 1 and Wee Waa

No. 1 wells, although Triassic sediments were not encountered in Baradine No. 1 well (20 miles east of Coonamble). Hind &

Helby {in Packham, 1969) have suggested that this unit com prises the Napperby Beds, the upper portion of the lower

Merrygoen Beds, the upper portion of the Lower Ballimore Beds and the Pottinger Beds.

This sequence is disconformably overlain, throughout the greater part of the area, by Early to Mid Jurassic sedi ments. However, the erosional break is marked by the extrusion of the Garrawilla Lavas in the Mullaley district. These lavas are extremely variable in their composition, ranging from olivine basalts to trachytes, often exhibiting extensive deuteric alteration. Kenny (1929) indicates that they attain a maximum thickness of 600 feet (180 m.). A detailed account of the distribution of these rocks is given by Dulhunty (1965,

1967). Potassium - argon dating of the flows in the Borah area indicates an age of about 181 million years (Dulhunty and

McDougal, 1966), suggesting a Late Triassic age, rather than a Jurassic age as commonly held. Recent mapping (Dr. J.

Dulhunty pers. comm.) confirms that the lavas are invariably found below sediments of undoubted Jurassic age. - 53-

Apart from "Estheria cf. mangalensis" which Dun (1909) illustrated with the Benelong plant collection faunal remains have not been recognised in this northern area. Plant fossils are relatively common in finer sediments, although data involv ing only a few collections are published. Hind & Helby (in

Packham, 1969) report a floral assemblage from the base of the

Wollar Sandstone at the Cox’s Gap Tunnel. The principal com ponents include Glossopteris spp., Cladophebis australis3

Schizoneura gondwanensis 3 ?Thinnfeldia oallipteroides and

Voltziopsis wolganensis. This assemblage is essentially similar to those encountered in the basal portion of the

Narrabeen Group. A further assemblage is reported from a number of localities in the vicinity of Dubbo (Dun, 1909,

Love and Bembrick, 1963 and Pickett, 1969). Principal elements of the flora include Dioroidium odontopteroides3 D. obtusifolium3

Baeria cf. multifida3 Ginkgo ? digitala3 Stenopteris rigida3

Strzleokia gangamopteroides and Taeniopteris spp. Overall this assemblage is reminiscent of the flora of the Ipswich

Coal Measures (Walkom, 1917), suggesting a probable Late

Triassic age. - 54-

2.2. DESCRIPTIVE PALYNOLOGY

The principal aim of this study is to establish a bio stratigraphy of the Late Permian-Triassic sediments of the

Sydney Basin. This biostratigraphy will be based on illu stration of the distribution of selected plant microfossils in time and space (set against the stratigraphic framework discussed above). The fundamental plant microfossil category on which the selection is based comprises the smallest morpho- graphically cohesive microfossil grouping which can be con stantly delineated with confidence.

At first sight this is an artifical concept. However, the individual microfossils which make up each category are discrete representatives, in some cases independently viable representatives, of more complex parent plants. As such, I would assume that they should reflect, in terms of their morphology, at least some influence of -

1. the environment in which the parent existed,

2. the maturity of the parent and certainly the relative

maturity of the spore or pollen bearing organ,

3. the relative evolutionary status of the parent plant,

although this would be relative to vertical sections only.

This is not to say that the parent will be identifiable in all instances from studies of the dispersed plant microfossils.

The gap in present knowledge concerning fossil spore and pollen bearing organs is manifestly large. However, even with a more comprehensive understanding of in situ plant microfossil to parent relationships the applicability of this data would still - 55- be limited. For example, extensive biometric and comparative studies of microspores extracted from fertile remains of seven

"species" of Coniopteris led Doludenko (1960) to conclude that representatives of the individual parent plants could not be identified confidently in dispersed assemblages. Similarly,

I believe that microspores comprising one of the morphological categories discussed above could represent a considerably more diverse parent group.

Traditionally these morphological categories are called form species. Despite the inherent artificiality of the con cept of form species the considerations outlined above suggest that a flexible delineation of the form species will serve in the best interests of a developing biostratigraphy.

In describing species below I have attempted to take into account the full variation encountered in successive populations. I have also attempted to illustrate as fully as possible the extent of these variations, particularly where previously undescribed species are involved or where concepts of a number of species or genera merge. Synonymy lists are not meant to be complete, but to trace the history of the specific epithet and encompass some of the more prominent cases of taxa which can not reasonably stand apart. I have assigned holotypes to conform to the regulations embodied in the present International Code of Botanical Nomenclature.

However, I regard the holotype merely as a convenient reposi tory for the specific epithet rather than a physical manifest ation of the concept of the species. I take this view because - 56- empirically the holotype specimen selected from a series of populations as defined by the morphographic range of the species is only a random variant. The possibility of subject ivity in the selection of holotypes, which is inherent in the type system, has been discussed by Hughes (1964).

Suprageneric terminology is used in this report only as a generalised guide to broader generic groupings. Apart from exine nomenclature, descriptive terminology is based on the glossaries presented by Dettmann (1963) and Kremp (1965).

I have cited references to most terms which do not appear in these works. Where exine layering has been detected, in both spores and pollen, the outer layer is described as the exoexine and the inner layer as the intexine. In no instance were more than two layers detected.

SYSTEMATICS

Anteturma SPORITES H. Potonie 1893

Turma TRILETES Reinsch emend. Dettmann 1963

Suprasubturma ACAVATRILETES Dettmann 1963

Subturma AZONOTRILETES Luber emend. Dettmann 1963

Infraturma LAEVIGATI Bennie & Kidston emend. R. Potonie 1956

Genus PUNCTATISPORITES Ibrahim emend.Potonie & Kremp 1954

Type species Punctatisporites punotatus Ibrahim - Original des ignat ion.

Remarks.

As emended by Potonie & Kremp (1954) the form genus

Punetatispov'ites encompasses spores of extremely simple - 57- organisation. Given the simplicity of this organisation there must be a distinct limit to the amount of diagnostic variation within the original concept. Despite these limitations the number of species assigned to Punotatisporites is prolific.

Punotatisporites is a constant and often significant component of Sydney Basin Late Permian - Triassic microfloras.

An extremely broad range of size (15-130 microns) and morpho logy is represented, apparently with complete gradations in most directions. I have been unable to satisfactorily delineate previously described Australian species from the total population.

Microspores which conform to Punotatisporites Ibrahim emend. Potonie & Kremp 1954 have been extracted from fertile remains of a fern described by Burges (1935) as Todites narrabeenensis. A number of these microspores are illustrated on

Plate . 1.

Punotatisporites sp. 1 PI. 1 Figs. 6-8.

Description of specimens.

Microspores, trilete. Amb. circular. Laesurae distinct, extend about 3/4 radius, accompanied by slightly raised lips, usually straight. Most specimens display a single arcuate fold close to the periphery. Exine 1-1.5 microns thick, smooth.

Dimens ions.

Equatorial diameter 30 (36) 40 microns. 20 specimens measure.

Comparisons.

This species is distinguished from previously described

Australian Punotatisporites species by its thinner exine and - 58-

relatively limited size range.

Occurrence.

Punctatisporites sp. 1 first appeared in the Gosford

Sub-Group and ranged through the Hawkesbury Sandstone, the

Wianamatta Group and their equivalents.

Punctatisporites subtvitus Playford & Helby

PI. 1 fig. 11.

1968 Punctatisporites subtvitus Playford & Helby, 107, pi. 9*

figs. 11, 12.

Description of specimens.

See Playford & Helby (1968, p. 107).

Remarks.

The specimens referred here to Punctatisporites subtvitus

Playford & Helby are indistinguishable from the Carboniferous population described by these authors (1968 , pp.107-108). The

presence of this form together with other diagnostic components

of the Grandispora microflora suggests that these specimens are probably reworked from a Carboniferous source area to the imme diate north of the sample area.

Occurrence.

Specimens of Punctatisporites subtvitus were identified

in samples 991 and 989.

Genus RETUSOTRILETES Naumova ex Potonie emend. Richardson 1965.

Type Species Retusotriletes simplex Naumova - designated by

Potonie (1958, p.13). Richardson (1965, p.563) designates

R. pychovii Naumova as type species. The reasons for this designation are not stated. - 59- Remarks.

The concept of Retusotriletes Naumova 1953 originally encompassed a broad range of forms characterised by distinct contact faces, usually delineated by perfect curvature. In validating the genus Potonie 1958 assigned it to the Infraturma

Laevigati, suggesting (by implication of this assignment) that the form should be confined to simple laevigate forms. Playford

(1964, p.9) has also commented on the desirability of restricting

Retusotriletes to laevigate species. Richardson (1965, p.563) proposed a formal emendation of the genus which excludes sculptured species. De Jersey (1966) rejected Richardson’s proposed emendation, arguing that some species with scabrate exine would be transitional between the laevigate and sculptured groupings.

Retusotriletes radiatus (Kara Murza) comb. nov.

PI. 1 Figs. 20,21,24,25.

Selected synonymy.

* ? 1951 Leiotriletes radiatus Kara Murza - not seen

1960 Leiotriletes radiatus Kara Murza, Tschalyschev & Vary-

ukhina, pi. 5 fig. 23.

1962 Leiotriletes radiatus Kara Murza, Tschalyschev & Vary-

ukhina, pi. 3 fig. 8

? 1964 Vaeneopsites luoida Malyavkhina, p. 50, pi. 13 fig. 18.

1966 Leiotriletes radiatus Kara Murza, Tschalyschev & Vary-

ukhina, pi. 2 figs. 9a, b.

? 1967 Stereisporites sp. de Jersey & Hamilton, p.4, pl.l fig.8.

* Footnote : Article not available. - 60-

Description of specimens.

Microspores, trilete, mildly patinate with perfect curvature. Laesurae straight or slightly sinuous, extend to proximal edge of patina (which is delineated by perfect curvature). Laesurae may be accompanied by slightly raised lips, varying from 0.5 - 2 microns in width, and merging onto patinal exine at the edge of the contact face. Exine of equatorial and distal surface 2-3 microns thick, dense simu lating a slightly developed patina. Patina extends into proximal surface, thinning abruptly at the edge of the contact area. Contact face relatively thin, often with scattered, very fine grana.

D imens ions.

33 (40) 45 microns - 25 specimens measured from sample 642.

Overall size range 26 - 48 microns.

Remarks.

Some specimens display a narrow, often wavy cingulum, suggesting a more complicated organisation than is normally assigned to Retusotrdletes. Comparisons. Retusotriletes radiatus (Kara Murza) comb. nov. differs from Limatulasporites fossulatus (Balme) comb. nov. in lacking a distal circumpolar incision in the patina. Forms referred by Tschalyschev & Varyukhina to Leiotriletes vadiatus Kara Murza are indistinguishable from the Sydney Basin forms (I have encountered this form in preparations kindly provided by Drs.

Tschalyschev & Varyukhina). A form described by Malyavkhina - 61-

(1964, p. 50) as Daeneopoites luoida is similar (although it was encountered in slightly younger sediments).

Occurrence.

Retusotviletes ? vadiatus (Kara Murza) comb. nov. is first encountered in sample 743, (lower Caley Formation) in Wollongong

D.D.H. No. 28. To date, it has not been identified from basal most Narrabeen Group microfloras, and is extremely rare above the horizon of the Bald Hill Claystone.

Genus PHYLLOTHECOTRILETES Luber 1955.

Type Species Phyllotheootviletes nigvitellus (Luber) Luber -

original designation.

Phyllotheootviletes nigvitellus (Luber) Luber.

PI. 1 figs. 12, 15-17

Selected Synonymy.

1941 Azonotviletes nigvitellus Luber (in Luber & Waltz), p.53,

pi. 12 fig. 180.

1946 Type P4d de Jersey, p. 4, p. 8 fig. 4d.

1952 Type P4d (de Jersey), Balme p. 7, fig. 4d.

1955 Phyllotheootviletes nigviteHus (Luber) Luber, p. 37, pi. 1

f ig. 6 .

1956b Calamospova diversifovmis Balme & Hennelly p. 246, pi. 2

figs.. 14-18

1962 Retusotviletes diver siformis (Balme & Hennelly,) Bharadwaj ,

p . 79

1965 Calamospova nigvitella (Luber & Waltz) Hart, p. 136,

text fig. 352 - 62-

Description of specimen.

Microspore, trilete, with characteristic contact area.

Amb circular to rounded triangular, varying within individual populations, outline often slightly irregular (pi. 1 fig. 12).

Laesurae distinct, straight varying in length from 1/3 to 3/4 radius. Contact area distinct, often exhibiting perfect cur vature (pi. 1 fig. 12) but usually defined as darkened sub- triangular area in the immediate vicinity of the proximal pole

(pi. 1 fig. 17). Exine smooth, microgranulate or punctate,

1.5 - 2 microns thick.

Dimensions.

30 (38) 54 microns. 10 specimens measured from sample 981.

Remarks.

Luber (1955) erected the genus Phyllothecotriletes ^ with

P. nigritellus (Luber) Luber as type species, to accommodate circular, smooth, thick exine forms with laesurae shorter than half radius. Luber's illustration of Azonotriletes nigritellus

(Luber 1941, pi. 12 fig. 180) displays a well defined, darkened, sub-triangular contact area. Specimens indistinguishable from the specimen illustrated by Luber occur throughout Australian

Permian microfloras. However, these specimens form a continuous morphological series with specimens which conform more readily to the concept of Retusotriletes Naumova emend. Richardson 1965.

Occurrence.

Phyllothecotriletes nigritellus is a relatively common component of Upper Permian coal measure microfloras. It extends into lower zonule of the Protohaploxypinus retieulatus Assemblage. - 63-

Rare occurrences of this form above the lower portion of the

Narrabeen Group are regarded as evidence of recycling.

Genus CYATHIDITES Couper 1953.

Type species. Cyathidites australis Couper - original des ignat ion.

Cyathidites breviradiatus Helby

PI. 1 figs. 2-5

1967 Cyathidites breviradiatus Helby, p. 63, pi. 1 fig. 4.

Remarks.

Cyathidites breviradiatus was diagnosed as possessing a smooth or faintly punctate exine (Helby 1967, p. 65). This diagnosis was based on examination of material from three samples. Examination of a much wider range of samples indicates that majority of forms referable to this species have a very finely granulate sculpture. The holotype exhibits a more or less smooth exine with a punctate structure. As indicated by de Jersey (1968, p. 4) this form has a wider size range than originally stated.

Occurrence.

Cyathidites breviradiatus Helby appears in the central portion of the Narrabeen Group, ranging through the Hawkesbury

Sandstone and Wianamatta Group as a rare component of the micro flora.

Genus DICTYOPHYLLIDITES Couper emend. Dettmann 1963.

Type species. Dictyophyllidites harrisii Couper - original

designation.

Dictyophyllidites harrisii Couper

PI. 1 figs. 18, 20. - 64-

1958 Diotyophyllidites harvisii Couper, p. 140, pi.21 figs.5.6.

Description of specimens.

See Couper (1958, p. 140).

Dimens ions.

Equatorial diameter 46 (56) 70 microns. 10 specimens measured from sample 547.

Polar diameter 45, 50, 68 microns.

Remarks.

The specimens assigned here to Diotyophyllidites harvisii

Couper have a slightly larger overall size range than the type population described by Couper (1958). In other respects they are indistinguishable.

Comparisons.

These forms are almost identical to Dioty ophyllidites mortoni (de Jersey) Playford & Dettmann. They are, however, locally abundant in the central portions of the Narrabeen Group and exhibit a slightly larger mean size and a noticeably thicker exine. As the latter features are not particularly diagnostic characters, these species are only tentatively separated.

Occurrence.

Dioty ophyllidites harvisii occurs intermittently throughout the Narrabeen Group, Hawkesbury Sandstone, Wianamatta Group and their equivalents. It is most prominently represented in the

Lunatisporites pelluoidus Assemblage and the Protohaploxypinus samoiloviohii Assemblage.

Dioty ophyllidites mortoni (de Jersey) Playford & Dettmann

PI. 1 figs. 9,10,13.14. - 65-

1953 Types 1C, 2C, 2E, 2H - Taylor, p. 156, 157, 158 figs. 1C, 2 C, 2 E, 2H.

1959 Leiotviletes movtoni de Jersey, p. 354, pi. 1 fig. 15.

1962 Concavispovites movtoni (de Jersey), de Jersey, p. 4, pi. 1 figs. 14, 15

1965 Dictyophyllidites movtoni (de Jersey), Playford & Dettmann, p. 132, pi. 12 figs. 1-3

Description of specimens.

See Playford & Dettmann (1965, p. 132.)

Dimensions.

Equatorial diameter 25 (34) 47 20 specimens measured.

Remarks.

De Jersey (1962, p. 4) has commented on the continuous

gradation of shape of Dictyophyllidites (Concavispovites) movtoni between concave and convex sides. Similarly, there is a wide

range of variation in the intensity and style of the folding which border the laesurae.

Previous Records.

Published data indicate that this species is a fairly con sistent component of eastern Australian Mid-Late Triassic micro floras .

Comparisons.

Dicty ophyllidites movtoni is tentatively distinguished from

D. havvisii Couper by its thinner exine and smaller mean size

(as compared with the local population).

Occurrence.

Dictyophyllidites movtoni is encountered as a rare component - 66-

of Late Permian coal measure microfloras in the Sydney Basin.

It extends throughout the Narrabeen Group, Hawkesbury Sandstone,

Wianamatta Group and their equivalents. It is least prominent

in the section below the base of the Falcisporites Assemblage

Zone .

Infraturma APICULATI Bennie and Kidston emend. Potonie 1956.

Genus GRANULATISPORITES Ibrahim emend. Potonie & Kremp 1954.

Type species. Granulatisporites granulatus Ibrahim - original des ignat ion.

Granulatisporites trisinus Balme & Hennelly

PI. 9 figs. 15, 16, 19-21.

1956b Granulatisporites trisinus Balme & Hennelly, p. 244, pi. 1 figs. 5-8

? 1962 Microfoveolatispora trisina (Balme & Hennelly) Bharadwaj, p. 82, pi. 3 figs. 50-53

Description of specimens.

See Balme & Hennelly 1956b. pp. 244, 245.

Remarks.

Balme & Hennelly (1956b, p. 245) have commented on the difficulty of resolving the sculpture of Granulatisporites trisinus. In many specimens the grana are scarcely raised above the surface of the exine, simulating a microfoveolate pattern in optical section. It is possible to ascertain the projecting nature of the sculpture on most specimens, but a few, possibly over-oxidised specimens, are indeterminate. The illustrations presented by Balme & Hennelly (1956b) are diffi cult to interpret. The specimen represented in fig. 5 (pi. 1) appears to have a microfoveolate exine. - 67-

Holotype.

Although Balme & Hennelly (1956b, p. 244) indicated a type locality for G. trisinus a holotype was not designated. Bharadwaj

(1962, p. 82) proposed the designation of an Indian specimen as "holotype" (lectotype) and on the basis of this illegitimate designation (Int. Bot. Code Article 7..) he recombined the species with Miorobaoul ispora Bharadwaj 1962. The specimen illustrated by Balme & Hennelly (1956b), pi. 1 fig. 5 is designated here as lectotype.

Occurrence.

Granulatisporites trisinus is a constant but minor component of Late Permian coal measure microfloras. It extends into the lower zonule of the Protohaploxypinus retioulatus Assemblage

Zone .

? Granulatisporites mioronodosus Balme & Hennelly

PI. 2 fig. 9,13,14,17,18.

Selected Synonymy.

1945 Type 26A Dulhunty, p. 155, text fig. 2.

1949 P 16A Dulhunty & Dulhunty, p. 135.

1952 P 27B Balme, p. 9, fig. 45.

1956b Granulatisporites mioronodosus Balme & Hennelly, p.245, pi. 1 f igs. 9,10.

Description of specimens.

Microspores, trilete. Amb convex triangular with rounded apicies. Laesurae more or less straight, extend almost to equator, accompanied by raised lips (2-4 microns high). Exine about 1 micron thick. Distal surface covered with closely - 68- packed (1-2.5 microns apart) baculae (1-2 microns high, 1-1.5 microns basal diameter). Sculptural elements extend onto

equatorial region of proximal surface diminishing rapidly in

size, interradial region smooth (pl.2fig.17 ). Compressions

in planes including polar axis relatively common.

Dimens ions.

Equatorial diameter 27 (37) 52 microns - 20 specimens measured.

Polar diameter 34 (52) 60 microns

Remarks.

In proposing Microbaculispora Bharadwaj (1962 , p. 80) designated M. gondwanensis as type species. The extremely short description of this species and the photograph of the holotype fail to distinguish it from Granulatisporites trisinus

Balme & Hennelly. The species concepts would appear to be identical. It is admitted that the type material of G. trisinus

(Balme & Hennelly 1956b, PI. 1 figs. 5-8) was poorly illustrated.

However, despite the clear descriptions of Balme & Hennelly

(1956b, pp. 244, 245) Bharadwaj (1962, p. 82) has attempted to recombine this species with Microfoveolatispora. The specimens illustrated as Microbaculispora gondwanensis Bharadwaj (1962 pi. 2 figs. 33-35) fall well with the limits of the G. trisinus population described above. The holotype of M. gondwanensis

Bharadwaj (pi. 2 fig. 33) does not illustrate smooth interradial area which Bharadwaj suggests is characteristic of the genus.

The concept of Microbaculispora described and illustrated by Bharadwaj (1962, p. 80; text fig. 4) obviously encompasses - 69- forms assigned here to ? Granulatisporites mioronodosus Balme &

Hennelly 1956b. However, as the validity of the genus is questionable the species G. mioronodosus is not combined with

Miorobaoulisp ora.

Occurrence.

? Granulatisporites mioronodosus Balme & Hennelly 1956b is a relatively rare but consistent component of the Dulhuntyispora

Assemblage and the Protohaploxypinus retioulatus Assemblage.

Genus CYCL0GRANISP0R1TES Potonie & Kremp 1954.

Type species. Cyologranisporites leopoldi (Kremp) Potonie & Kremp - original designation.

Cyologranisporites sp. 1

PI. 2 figs. 10

Description of specimens.

Microspores, trilete. Amb circular, periphery dentate.

Laesurae usually extinct, simple extend about 2/3 radius. Exine

1.5-2 microns thick, not noticeably layered, bearing grana and small coni (0.5-1 micron basal diameter; 1-1.5 microns in height;

1-2 microns apart.

Dimens ions.

Equatorial diameter 26 (31) 35 microns. 10 specimens measured.

Remarks.

This species is characterised by the consistent rounded out line of the sculptural elements and the narrow size range

(despite wide occurrence).

Comparisons.

Cyologranisporites minutus Bharadwaj has shorter laesurae, - 70-

finer and more closely packed grana. Cyelogranisporites

leopoldi (Kremp) Potonie & Kremp is very similar. Cyelo- granisporites avenosus Maedler has a much thicker exine.

Occurrence.

Cyelogranisporites sp. 1 occurs intermittently throughout

the Narrabeen Group, attaining maximum prominence in samples of

the Lunatisporites pellueidus Assemblage and the Protohaploxy - pinus samoiloviehii Assemblage.

Genus 0SMUNDACIDITES Couper 1953.

Type species. Osmundaeidites wellmanii Couper - original designation

Remarks.

There exists an obvious overlap in the morphological con

cepts of Cy elogranisporites Potonie & Kremp 1954 and Osmunda- c-idites Couper 1953 . Balme (1963) cites the diversity of sculptural elements on single specimens of 0smundacidites as a diagnostic distinguishing feature. If the variability of the sculptural elements is accepted as a diagnostic generic character than its significance at specific level is surely limited.

0smundacidites wellmanii Couper

PI. 2 figs. 11. 12.

1953 Osmundaeidites wellmanii Couper, p. 20, pi. 1 fig. 5.

Remarks.

Osmundaeidites wellmanii is almost ubiquitous throughout tie section. Forms assigned to the species include a vast range oi morphological variation. I have insuccessfully attempted to - 71- divide the population on the basis of numerous parameters including size, length of laesurae and nature of sculptural organisation. Playford (1965, p. 182) has previously commented on the extremely broad morphological range of 0. wellmanii.

Couper (1958, p. 134) comments that "0. wellmanii affords a good example of the broadness of spore species".

Previous records.

0smundaeidites wellmanii occurs extensively throughout

Mesozoic strata. Balme (1970) reports a possibly synonymous form - 0. s eneotus Balme from the Late Permian Chhidru Formation of Pakistan and the Scythian Kockatea Shale of the Perth Basin.

Occurrence.

0smundaeidites wellmanii occurs in nearly all samples investigated. It is often the dominant pheridophytic element in microfloras above the base of the Gosford Sub-Group and extending through the Hawkesbury Sandstone, Wianamatta Group and their equivalents.

Genus APICULATISPORIS Potonie & Kremp 1956.

1933 Apieulatisporites (partim) Bennie & Kidston 1886, Ibrahim

p . 23

1954 Apieulatisporites Ibrahim 1933, non Bennie & Kidston emend.

Potonie & Kremp. p. 130

1956 Apieulatisporis Potonie & Kremp, p. 94

Type species. Apieulatisporis aeuleatus (Ibrahim) Potonie & Kremp

- original designation (see Potonie & Kremp 1956,

p . 94 )

Apieulatisporis bulliensis Hennelly emend.

PI. 2 figs. 1 - 8

1958 Apieulatisporites bulliensis Hennelly, p.364 , pi.5 figs.3-5. - 72-

Description of specimens.

Microspores, trilete, outline round to oval, occasionally

rounded triangular. Laesurae vary from indistinct to prominent,

often slightly sinuous, extend about 3/4 radius. Lips not

apparent in all assemblages up to 1.5 microns high, 0.5-1 micron wide. Exine not noticeably layered, 1.5-2 microns thick,

distal and equatorial surfaces covered with spines. Contact

face smooth. Spines 1-3 microns apart (varies considerably from

specimen to specimen), usually more densely packed in vicinity

of the distal pole. Spines up to 2.5 microns long, 0.5-1.5 microns basal diameter, tapering rapidly at a height of 1-1.5 microns to an attenuated point (see PI. 2 fig. 3). Coni occur on less well preserved specimens.

Dimensions.

Equatorial diameter. 18 (26) 40 microns - 50 specimens measured from sample 628.

18 (27.5) 37 microns - 30 specimens measured from sample 689.

23 (29) 35 microns - 30 specimens

measured from sample 985.

Remarks.

The Apiculatisporis bull'iensis populations described above represent a considerably broader morphological group than that outlined by Hennelly (1958, p. 364). The differences could possibly be related to the preservation of the assemblages, although a full morphological range is represented in Hennelly's material. The presence or absence of lips accompanying the laesurae would appear to have limited significance. The nature - 73- of the spines almost certainly results in loss of the attenuated pointed section in cases of adverse preservation conditions.

Comparisons.

Apioulatisporis bulliensis is morphologically similar to

Apioulatisporis levis (Balme & Hennelly) Hart (this form could possibly be assigned to Anaplanisporites Jansonius 1962). How ever, it would appear to have a thicker exine, longer laesurae and a distinctly spinose sculpture, although it is not possible at this time to comment on the relative preservation of the material described by Balme & Hennelly (1956b, p. 246).

Occurrence.

Apioulatisporis bulliensis is first encountered immediately above the Bulli Seam - Nattai Seam - Katoomba Seam of the

Illawarah Coal Measures and the Vales Point Coal Member in the basal section of Munmorah Conglomerate. It is particularly abundant in the lower zonule of the Protohaploxypinus vetioulatus and occurs Assemblage Zone^ intermittently through to the Protohaploxypinus samoiloviohii Assemblage Zone.

Apioulatisporis oarnarvonensis (de Jersey & Hamilton) comb. nov.

PI. 3 figs. 9-11, 13.

1967 Verruoosisporites oarnarvonensis de Jersey & Hamilton, p. 6, PI. 2 figs. 1-5

Description of Specimens.

See de Jersey & Hamilton (1967, p.6)

Dimens ions.

Equatorial diameter 52 (74) 110 microns - 25 specimens measured. - 74-

Remarks .

From the various interpretations of verruoae cited by Kremp

(1965, p. 175) it is clear that most authors regard this sculp tural feature as having a greater basal diameter than height.

In cases where opinion digresses slightly, the irregularity of the feature in plain view is stressed. The sculptural ele ments of forms illustrated by de Jersey & Hamilton (1967, pi. 2 figs. 1-5) as Verruoosisporites oarnarvonensis are almost exclusively conate. This species is therefore re-assigned to Apiculatisporis Potonie & Kremp 1956 .

The specimen designated as holotype of Apioulatisporis oarnarvonensis (de Jersey & Hamilton 1967, pi. 2 figs. 1-5) although distinctly and predominantly conate has considerably shorter coni than other specimens illustrated by those authors.

It is not possible to determine from the description and remarks of the authors if the holotype was representative of the total population of A. oarnarvonensis in their Moolayember Formation material. The development of coni on the majority of specimens recovered from sub-surface Moolayember Formation in northern

New South Wales, the Hawkesbury Sandstone and Wianamatta Group of the Sydney area is more pronounced. The specimen designated as holotype would be close to an end member of the coni devel opment range of the population studied here. These end members are similar to Verruoo sisporites pseudomoruZae Visscher, but distinguished by structure of the sculptural elements.

Occurrence.

Apioulatisporis oarnarvonensis first appears in the Hawkes- - 75- bur y Sandstone and its equivalents and is a fairly constant

component of Wianamatta Group microfloras.

Apioulatisporis globosus (Leschik) Playford & Dettmann

PI. 3 f igs . 1-3 , 5-7

1955 Apioulatisporites globosus Leschik, p. 18, pi. 2 fig. 8

? 1958 Braoteolinasporites olavatus Nilsson, p. 48, pi. 3 fig. 1

1968 Apioulatisporis olematisi de Jersey, p. 6, pi. 1 fig. 12. 1965 Apioulatisporis globosus(Leschik) Playford & Dettmann, Description of specimens. p.137, pi. 16, figs. 16-18.

Microspores, trilete. Amb circular to convex triangular with rounded apices. Laesurae seldom distinct, simple or

slightly raised lips. Exine 1-2 microns thick bearing wide variety of sculptural elements including spines (up to 6 microns long, 2 microns basal diameter) baculae (up to 4 microns long, 3 microns basal diameter) on single specimens.

Size of sculptural elements diminishes approaching laesurae.

Sculptural elements diminishes approaching laesurae. Sculptural

elements closely packed, seldom more than 2 microns apart at

the bases.

Dimens ions.

Equatorial diameter 30 (52) 67 microns - 20 specimens measured.

Remarks.

Specimens assigned here to Apioulatisporis globosus (Leschik)

Playford & Dettmann exhibit an extremely wide range of size and form of sculptural elements. This range obviously covers the population described by Playford & Dettmann from the Leigh Creek

Coal Measures and also the Apioulatisporis olematisi de Jersey - 76- specimens from the Clematis Sandstone. However, the illus tration of the holotype of A. globosus (Leschik, pi. 2 fig. 8) scarcely supports a suggestion of variable sculpture. Should further elucidation of the morphology of A. globosus require separation of the Australian forms A. olematisi de Jersey would assume priority.

Occurrence.

Apioulatispovis globosus is first encountered in the

Newport Formation and extends through the Hawkesbury Sandstone,

Wianamatta Group and their equivalents.

Apioulatispovis sp. 1

PI. 4 figs. 6,7.

Description of specimens.

Microspores, radial, trilete. Amb circular, periphery dentate due to projecting sculpture. Laesurae extend 1/2 -

2/3 radius. Exine about 1 micron thick bearing spines 3-4 microns long 1.5 microns basal diameter, very closely packed.

Sculptural elements absent from immediate vicinity of laesurae.

Dimens ions.

Equatorial diameter 31-45 microns.

Comparisons.

Apioulatispovis filifovmis Balme & Hennelly has similar but less closely packed spines. The laesurae of this form also extend to the periphery.

Occurrence.

Apioulatispovis sp. 1 occurs as a rare component of basal

Narrabeen Group microfloras. - 77- Apieulatispovis sp. 2

PI. 3 figs. 4,8,11; PI. 4 figs. 1,10,14.

Description of specimens.

Microspores, trilete. Amb circular to sub-triangular with convex sides and rounded corners, periphery irregular due to projecting sculpture. Distal surface fully hemispherical, proximal surface forms a low pyramid in lateral view. Laesurae seldom distinct, simple extending 2/3 to 3/4 radius. Exine not noticeably layered, bearing very closely packed, discrete coni

(up to 3 microns basal diameter up to 5 microns high) and spines with rounded tips (up to 5 microns long, 2-3 microns basal diameter) on distal and equatorial surfaces. Structural ele ments often blunted. Proximal surface smooth in vicinity of the apex.

Dimensions.

Equatorial diameter 35 (50) 63 microns. 7 specimens measured.

Polar diameter 49 microns. 1 specimen measured.

Remarks.

Apicutatisporis sp. 2 is a very distinctive form which appears to have a restricted zone of occurrence. However, insufficient forms were recorded to allow formal description.

Comparisons.

Neoraistriekia pioketti sp. nov. has a less closely spaced sculptural elements which are predominantly baculate and pilate.

Apioulatisporis globosus (Leschik) emend. Playford & Dettmann displays a greater range of sculptural elements on individual specimens. - 78-

Occurrence .

Apiculatisporis sp. 2 is a rare component of microfloras from the upper portion of the Hawkesbury Sandstone, extending into the Bringelly Shale. A single specimen also occurred in the upper portion of the Wollar Sandstone.

Genus ACANTHOTRILETES Naumova emend. Potonie & Kremp 1954.

Type species. Acanthotriletes ciliatus (Knox) Potonie & Kremp -

designated by Potonie & Kremp 1954, p. 133.

Remarks.

Acanthotriletes is a rather loosely defined genus encom passing trilete microspores with closely packed, tapered spines,

the basal diameter of which is less than half the length. It is this ratio of basal diameter; length of the spines which distinguishes the genus from Lophotriletes Naumova emend.

Potonie & Kremp 1954 and Apiculatisporis Potonie & Kremp 1956.

Acanthotriletes hennellyi sp. nov.

PI. 4 figs. 12, 13, 16, 17.

1962 Acanthotriletes sp. - Bharadwaj, pi. 1 fig. 23

1967 Acanthotriletes tereteangulatus Balme & Hennelly -

Balme & Playford, p. 181, pi. 1 fig. 4.

Description of specimens.

Microspores, trilete. Amb sub-triangular, usually with convex sides but varying to concave sides, rounded apices.

Laesurae simple, slightly sinuous extending almost to periphery.

Exine thin, about 1 micron, not noticeably layered, distal and equatorial surface bear scattered (3-4 microns apart) spines,

3-8 microns in length, 1.5 - 3 microns basal diameter. Spines - 79- taper gradually, although tips occassiona1ly broken off.

Sculpture less prominent approaching laesurae.

Dimens ions.

Equatorial diameter 20 (31) 38 microns (exclusive of sculpture) 20 specimens measured from sample 628.

Type locality.

Newvale No. 28 D.D.H. at 301 ft. (Karignan Conglomerate)

Holotype.

Slide 992/1 25.4 118.7, Illustrations - PI.4 figs. 13. 17

Comparisons.

Balme & Playford (1967, p. 181) indicate a broad range of sculptural elements, often on a single specimen, as characte ristic of ? Acanthotriletes tereteangulatus Balme & Hennelly.

The specimen illustrated by those authors (pi. 1 fig. 4) dis plays a predominantly spinose sculpture in which the ratio- spine length to basal diameter - would appear to exceed 3.1.

This is a marked contrast to the type population described and illustrated by Balme & Hennelly (1965b) which appears to have a predominantly conate sculpture with intermittent spines. The spines of 1A. tereteangulatus taper rapidly above a broad, almost conate base (see Balme & Hennelly pi. 2 fig. 29). I have not been able to establish a gradation between these species.

Occurrence.

Acanthotriletes hennetlyi was first encountered, in this study, in the Dulhuntyispora Assemblage Zone. It is a relative ly rare but persistent component of the Dulhuntyispora and - 80-

Protohaploxyp'inus reticulatus assemblages. It extends into

the Protohaploxypinus samoiloviohii Assemblage Zone.

Acanthotriletes prospeotensis sp. nov.

PI. 4 figs. 4, 5, 8, 9.

Description of specimens.

Microspores, trilete. Amb triangular, sides predominantly

concave with rounded corners, periphery interrupted by pro

jecting sculpture. Distal surface almost hemispherical (vary

ing to conate) proximal surface pyramidal in lateral view.

Laesurae distinct, simple (although some specimens take up

extra stain immediately adjacent to laesurae) extending 2/3

to 3/4 radius. Exine not noticeably layered, bearing small

spines (1.5-2 microns apart). Sculpture extends onto proximal

surface but diminishing in size approaching laesurae. Exine

less than 1 micron thick.

Dimensions.

Equatorial diameter 25 (29) 34 microns. 30 specimens measured from sample 760.

Polar diameter 23 - 32 microns.

Type locality.

Prospect Reservoir, Liverpool 1 mile G.R. 874 210. (Bringelly Shale)

Holo typ e.

Slide 760/1 33.0 104.0 Illustrations - PI. 4 figs. 5, 9 (27 microns)

Remarks.

Spines on poorly preserved specimens are often broken, giving the impression of a granulate sculpture. - 81-

Comparisons .

Acanthotriletes prospectensis sp. nov. superficially resembles the specimen of Lophotritetes sparsus illustrated by Singh (1964, pi. 44 fig. 23), but has finer, more closely packed, spinose sculptural elements. Acanthotriletes teretean gulatus Balme & Hennelly has longer laesurae (significance uncertain) and considerably coarser sculptural elements.

Lophotriletes novicus Singh has a considerably larger mean size and predominantly conate sculpture.

Occurrence.

Acanthotriletes prospectensis sp. nov. is first recognised in the central portion of the Hawkesbury Sandstone, and extends into the Bringelly Shale of the Wianamatta Group.

?Acanthotriletes tereteangulatus Balme & Hennelly

PI. 4 figs. 2, 3.

Selected Synonymy.

1952 P 17 B Balme, p. 8, fig. 43 - P 17 B

1954 Raistrickia sp. - Rilett, p. 35, pi. 5 fig. 1

1956b Acanthotriletes tereteangulatus Balme & Hennelly, p. 247, pi. 2 figs. 27-29.

Description of specimen.

Microspore, trilete. Amb triangular, sides ususally slightly concave, apices rounded. Laesurae variable, straight or sinuous, extend 2/3 - 3/4 radius, accompanied by slightly thickened exine, rim up to 3 microns wide. Exine about 1 micron thick, not noticeably layered bearing cones and spines. Coni 1.5 - 3 microns high, 1 - 2.5 microns basal diameter, spines up to 4 microns - 82- microns long 2 microns basal diameter but tapering rapidly immediately above base, 1-3 microns apart.

Dimensions.

Equatorial diameter 23 (32) 39 microns - 10 specimens measured.

Remarks.

It is difficult to ascertain whether the type material of

Aoanthotriletes teveteanguZatus Balme & Hennelly actually conforms to the concept of AeanthotviZetes Naumova as emended by Potonie & Kremp (1954). Many specimens would be more suitably accomodated by LophotviZetes Naumova emend. Potonie

& Kremp 1954.

Previous Records.

Balme (1970) has suggested that AeanthotvZZetes teretean- guZatus is ubiquitous in Australian Permian microfloras. A morphologically similar form, AzonotviZetes trZsuZcus is reported by Andreeva et aZ. (1956, p. 244, pi. 47, figs. 33a, b) .

Occurrence.

? AeanthotviZetes tevteanguZatus Balme & Hennelly was encountered in all samples between and including the Wallarah

Seam and the Vales Point Coal Member. It is a fairly constant component of the lower zonule of the PvotohapZoxypinus vetieuZatus

Assemblage Zone.

Genus DIDECITRILETES Venkatachala & Kar 1965

Type species. DideeitriZetes hovridus Venkatachala & Kar 1965 - original designation. - 83-

Remarks .

Venkatachala & Kar (1965, p. 338) proposed the form genus

Dideoitritetes to accommodate trilete microspores, with tri angular amb, prominent laesurae "accompanied by folds" and spinose sculpture which diminish in size and density approach ing the proximal apex. They suggest that the genus is similar in organisation to Miorobaoulispora Bharadwaj 1962, although this latter form has smooth contact faces (Bharadwaj 1962, p. 80; text fig. 4). They attempt to distinguish Anapioula- tisporites Potonie & Kremp 1954 by the absence of the "folds" accompanying the laesurae and indicate that Anapioulatisporites is characterised by a smooth proximal surface. This differs from the description of Potonie & Kremp (1954 p. 130) "....

Proximalseite in Bereioh der Dehiszenzmarke glatt ....", which suggests to me an organisation similar to Miorobaoulispora

Bharadwaj (1962, text fig. 4). Also, in referring Aoanthotriletes erioianus Balme & Hennelly to Dideoitritetes Venkatachala & Kar have included a form which may exhibit psilate proximal, interradial surfaces or alternatively display decreasing density and size of spines approaching the proximal pole (see Balme &

Hennelly, 1967b, p. 249).

Although I reject the distribution of the sculptural ele ments as a particularly diagnostic feature, the nature of the trilete mark is quite characteristic. A distinct suite of

Apiculati microspores is encountered in southern continents and some Angaraland Mid to Late Permian microfloras. However, in most cases I interpret these forms as having raised labrae -84 rather than folds accompanying the laesurae. These forms are tentatively assigned to Dddeodtvd'ietes Venkatachala & Kar 1965 .

Dddeodtvd'iete s evdcdanus (Balme & Hennelly) Venkatachala & Kar.

PI. 4 f igs. 18-20

Selected Synonymy.

1945 Type 16A Dulhunty, p. 154, text fig. 2, pi. 7 fig. 16A.

1946 P. 16A (Dulhunty) de Jersey, p.

1956b Acanthotvdletes evdodanus Balme & Hennelly, p. 218, pi. 3 f igs. 30-33 .

1962 Anapdoulatdspordtes evdodanus (Balme & Hennelly) Bharadwaj, p . 79

1965 Dddeodtvdietes evdodanus (Balme & Hennelly) Venkatachala & Kar, p. 338

Description of specimen.

See Balme & Hennelly 1956b, p. 248.

Holotype.

Although Balme & Hennelly (1956b, p. 248) indicated the seam at 755 ft.,Newstan D.D.H. No. 2 as type locality, a holotype was not designated. Venkatachala & Kar (1965, p. 339) have assigned the specimen illustrated by Balme & Hennelly

(1956b) on pi. 3 fig. 30 as "holotype" (lectotype).

Comparisons.

Dddeodtvdietes evdodanus (Balme & Hennelly) Venkatachala

& Kar is distinguished from D. dentatus (Balme & Hennelly)

Venkatachala & Kar by its smaller, more numerous spines. It is similar to D. horrddus Venkatachala & Kar and I am not sure that these forms can be satisfactorily delineated. Azonotrdletes tenudspdnosus Waltz (dn Luber & Waltz 1941) is also similarly - 85- organised.

Occurrence.

Dideeitvttetes evicianus (Balme & Hennelly) Venkatachala

& Kar is a minor but common component of Late Permian coal measures and basal Narrabeen Group microfloras of the Sydney

Bas in. didecitriletes sp. cf. D. dentatus (Balme & Hennelly) Venka tachala & Kar . PI. 4 f igs. 11. 15.

1956b Acanthotviletes dentatus Balme & Hennelly, p. 248, pi. 3 f ig. 34.

1962 Anapieulatisporites dentatus (Balme & Hennelly) Bharadwaj, p. 79

1965 dideoitv'i’letes dentatus (Balme & Hennelly) Venkatachala & Kar, p. 339.

Description of specimens.

See Balme & Hennelly 1956b, p. 248.

Remarks.

The specimens referred here to Didec'itv'iletes sp. cf.

D. dentatus have a smaller size range (52, 74 microns) than

that indicated by Balme & Hennelly, (1956b, p. 248). However,

the nature of the spines (4-6 microns long, 2.5-3.5 microns

at the base) is essentially similar to D . dentatus.

Occurrence.

Several specimens of Didec'itv'i'letes sp. cf. D. dentatus

(Balme & Hennelly) Venkatachala & Kar were encountered in

sample 327 from basal Narrabeen Group sediments at Cox’s Gap. - 86-

Genus RAISTRICKIA Schopf et al. 1944 emend. Potonié & Kremp 1954

Type species. Raistriekia grovensis Schopf (in Schopf et al. 1944) - original designation.

Raistriekia aeeineta Playford & Helby

PI. 6 fig. 12

1968 Raistriekia aeeineta Playford & Helby, p. 109, pi. 9 figs. 13. 14.

Description of specimens.

See Playford & Helby (1968, p. 109)

Remarks.

The specimens assigned here to Raistriekia aeeineta Play

ford & Helby are indistinguishable from the Carboniferous

population described by those authors (1968, p. 109). The

presence of this form and other diagnostic components of the

" Grandispora" microflora (Helby, 1969) suggests that these

specimens are probably reworked from Carboniferous source areas

to the immediate north of the sample area.

Occurrence.

Raistriekia aeeineta was encountered in samples 991 and 992,

between the Wallarah Seam and the Vales Point Coal Member, in

Newvale D.D.H. No. 28, and sample 591 in the basal portion of

the Munmorah Conglomerate in Ourimbah Creek D.D.H. No. 5.

Raistriekia radiosa Playford & Helby

PI. 6 f ig. 3

1968 Raistriekia radiosa Playford & Helby, p. 109, pi. 9 figs. 8-10.

Description of specimens.

See Playford & Helby 1968. - 87-

Remarks .

The specimens assigned to Raistriokia radiosa Playford &

Helby are indistinguishable from the Carboniferous population

described by those authors (1968, p. 109-110). The presence

of this form and other diagnostic components of the Grandispora microflora suggests that these specimens are recycled from

Carboniferous source areas to the immediate north of the sample

locations.

Occurrence.

Several specimens of Raistriokia radiosa were encountered

in sample 991.

cf. Raistriokia sp.

PI. 5 figs. 1, 2.

Description of specimens.

Microspores, trilete. Amb circular to sub-triangular, periphery irregular due to projecting sculptural elements.

Laesurae seldom distinct, simple, extend 2/3 radius. Exine not noticeably layered, thick, 3 microns exclusive of sculpture.

Exine bearing baculae (2-6 microns basal diameter, 3-6 microns high often with expanded castellated extremities - up, to 7 microns across), coni (3-5 microns basal diameter, 4-5 microns high), verrucae (shape irregular, basal diameter up to 4 microns) and low rounded rugulae of irregular outline. Bases of sculp tural elements occasionally anastomose on distal and equatorial surfaces, although bases of elements can be 8 microns apart, sculptural elements diminish in size approaching laesurae, which are often bordered by small irregular verrucae and grana. - 88-

D imensions.

65 — 82 microns.

Remarks.

A restricted number of specimens of cf. Raistriokia sp. are recorded. However, this is a distinctive form and appears to have a narrow range of occurrence. There is some doubt con cerning the referral of these forms to Raistriokia due to irregular often indiscrete nature of the sculptural elements.

Occurrence.

cf. Raistviokia sp. is a very rare component of basalmost

Narrabeen Group microfloras.

Genus BACULATISPORITES Thomson & Pflug 1953

Type species. Baoulatisporites primarius (Wolff) Thomson & Pflug - original designation.

?Baculat'isporites wianamattaense sp. nov.

PI. 6 figs. 4, 5, 8, 10, 11.

Description of specimens.

Microspore, radial, trilete. Amb circular to sub-triangular, periphery irregular due to projecting sculptural elements.

Laesurae distinct, accompanied by slightly raised membranous lips, more or less straight, extending 2/3 to 3/4 radius.

Contact area usually marked by folding. Exine 1-2 microns thick, bearing variety of sculptural elements on distal and proximal equatorial surfaces. Sculptural elements comprised of baculae (3-7 microns long, 1.5-4 microns basal diameter), coni (2.5-5 microns high, 2-4 microns basal diameter) small spines and occasional irregular verrucae. Sculptural elements discrete, bases 0.5-1 micron apart, diminish in size approaching - 89-

apex.

Dimens ions.

Equatorial diameter 57 (67) 81 microns. 20 specimens measured from sample 429.

Type locality.

Prospect Reservoir Treatment Plant, D.D.H. No. 13 at 35 ft. (Bringelly Shale).

Ho 1o t yp e .

Slide 429/1 39.6 1080. Illustrations - PI. 6 fig. 10

Remarks.

These specimens are assigned to Baculatisporites Thomson & Pflug 1953 rather than Apiculatisporis Potonie & Kremp 1956

because of the predominance of baculate sculptural elements.

Potonie (1956, p. 33) indicates that the holotype of Bacula

tisporites primarius (Wo 1 f f) Thomson & Pflug exhibits both

baculate and conate sculpture. The occurrence of a folded

rim around the contact area is reminiscent of the proximal

circumpolar murus of Cadargasporites de Jersey & Paten emend.

The extension of sculptural elements on to the contact area would not necessarily exclude this species from Cadargasporites.

However, convincing evidence of layering of the exine has not been seen.

Comparisons.

Baoulatisporites wianamattaense sp. nov. differs from

Apiculatisporis globosus (Leschik) Playford & Dettmann in having more massive, closely packed, predominantly baculate sculptural elements. Cadargasporites seneotus de Jersey &

Hamilton has a membranous proximal circumpolar murus, and - 90- considerably finer sculptural elements. Guttatisporites grandis sp. nov. lacks a distinct contact area and has more massive sculptural elements.

Occurrence.

Baeulatisporites wianamattaen.se sp. nov. is first recognised in the Bringelly Shale. It appears to be confined to the

Wianamatta Group.

Genus LOPHOTRILETES Naumova emend. Potonie & Kremp 1954.

Type species. Lophotriletes gibbosus (Ibrahim) Potonie &

Kremp - designated by Potonie & Kremp (1954,

p. 129).

Lophotriletes novieus Singh

PI. 5 figs. 3, 4, 7, 10, 11.

Selected Synonymy.

? 1953 Type 26A - Taylor, p. 159, p. 160 fig. 26A.

1964 Lophotriletes novieus Singh, p. 241, pi. 44 figs. 24, 25.

1967 Lophotriletes bauhiniae de Jersey & Hamilton, p. 7,

p. 3 figs. 3, 5, 7-9.

Description of specimens.

See Singh (1964, p. 247).

Dimensions.

Equatorial diameter 33 (46) 55 microns. 20 specimens

measured from sample 482.

Co mp ar is ons.

Apart from the slightly larger mean size Lophotriletes bauhiniae de Jersey & Hamilton is indistinguishable from

L. novieus Singh. Balme (1970) suggested that L. novieus - 91- may be a junior synonym of L. varus Bharadwaj & Salujha, although the illustrations of this latter form are inadequate for satisfactory comparison. The form illustrated by Taylor

(1953, p. 160 type 26A) would appear to conform to the concept of L. novious.

Previous Records.

Lophotriletes novious Singh is reported from the Late

Permian Chia Zairi Formation of northern Iraq (Singh, 1964) the Early Permian Amb Formation, and the Late Permian Wargal

Limestone and Chhidru Formation of the Salt Range (Balme,1970).

It is reported from the Moolayember Formation (de Jersey &

Hamilton, 1967), the Clematis Sandstone (de Jersey, 1968) and the Wandoan Formation (de Jersey & Hamilton, 1969) of south eastern Queensland.

Occurrence.

Lophotriletes novious Singh was first encountered in sedi ments immediately below the Vales Point Coal Member. It is a fairly consistent component of lower Narrabeen Group microfloras, decreasing in prominence up the Narrabeen Group section. It is a common component of Hawkesbury Sandstone and Wianamatta Group assemblages, attaining maximum prominence in the lower portion of the Wianamatta Group.

Genus CAMPTOTRILETES Naumova ex Potonie & Kremp 1954

Type species. Camptotriletes oorrugatus (Ibrahim) Potonie &

Kremp - designated by Potonie & Kremp (1954 p.142)

Camptotriletes sp. cf. C. warohiana Balme

PI. 6 figs. 6, 7, 9. - 92-

1970 Camptotritetes warohiana Balme, p. , pi. 3 figs. 12, 13.

Description of specimens.

See Balme, 1970.

Dimens ions.

Equatorial diameter 43 - 72 microns.

Remarks.

The specimens assigned to this category display a broad range of sculptural elements, similar to the population of

C. warohiana described by Balme (1970). The Sydney Basin population would appear to have a smaller size range and mean size.

Previous records.

Balme (1970) initially reported the occurrence of Campto- triletes warohiana in the Permian Amb and Chhidru Formation of

Pakistan.

Occurrence.

Camptotriletes sp. cf. C. warohiana was first recognised in microfloras from the Vales Point Coal Member. It is a rare component of basalmost Narrabeen Group microfloras.

Genus VERRUCOSISPORITES Ibrahim emend. Potonie & Kremp 1954

Type species. Verruoosisporites verrucosus Ibrahim - original

des ignat ion.

Verruoosisporites sp. cf. V. trisecatus Balme & Hennelly

PI. 5 figs. 5, 6, 8, 9.

1956b Verruoosisporites trisecatus Balme & Hennelly, p. 250.

pi. 4 figs. 48, 49. pi. 5 fig. 50.

Remarks.

Specimens assigned to this category conform closely to the - 93- concept of Vevvuoosispovites tvis eoatus outlined by Balme &

Hennelly. However, several specimens (in particular pi. 5 fig. 5) suggest that this form has a distinctly layered, but acavate exine.

Previous record.

Balme & Hennelly record V. tviseoatus from the Mid to Late

Permian Newcastle & Tomago Coal Measures. They also infer it’s occurrence in the probable Late Permian Liveringa Formation of

Western Australia.

Occurrence.

Vevvuoosispovites sp. cf. V. tviseoatus was first recog nised in the microflora from the Vales Point Coal Member. It is a rare but fairly consistent component of the lower zonule of the Pvotohaploxypinus vetioulatus Assemblage Zone.

Vevvuoosispovites sp. cf. V. gobbettii Playford.

PI. 6 fig. 13.

1962 Vevvuoosispovites gobbettii : Playford, p. 586, pi. 80

figs. 1-4.

Description of specimens.

See Playford & Helby (1968, p. 100)

Remarks.

The specimens assigned to Vevvuoosispovites sp. cf.

V. gobbettii above are indistinguishable from the Carboniferous population described by Playford & Helby (1968, pp. 108-109).

The presence of numerous other diagnostic components of the

Gvandispova microflora (Helby, 1969) suggest that these speci mens are probably reworked from Carboniferous source areas to the immediate north of the sample location. - 94-

Occurrence .

Well preserved specimens assigned to Vevvueosispovites sp. cf.

V. gobbettii Playford were encountered in samples 991 and 992 , between the Wallarah Seam and the Vales Point Coal Member in

Newvale D.D.H. No. 28.

Genus CLAVATRILETES Herbst 1965

Type species. Clavatviletes hammenii Herbst - original designation.

Clavatviletes sp. cf. C. hammenii Herbst

PI. 6 figs. 1, 2.

1965 Clavatviletes hammenii Herbst, p. 144, pi. 1 fig. 7; pi. 2

figs. 14, 15. non 1968 Clavatviletes hammenii Herbst, auet. non. Jain, p. 14,

pi. 1 f ig . 26 .

Remarks.

Specimens assigned to this category conform closely to similarly designated forms from the Moolayember Formation of southern Queensland (de Jersey & Hamilton, 1967, p. 6). This population appears to be slightly larger and exhibits a sculp tural diversity which may differentiate it from the type material.

Previous Records.

Herbst originally described this C. hammenii from the Los

Rastros Formation (?Norian) of Argentina. Forms designated as C. sp. cf. C. hammenii are reported from the Clematis Sand stone, Moolayember Formation and Wandoan Formation of southern

Queensland (de Jersey, 1968; de Jersey & Hamilton 1967, 1969).

Occurrence.

Clavatviletes sp. cf. C. hammenii was first identified in the Newport Formation of the Narrabeen Group. It occurs inter- - 95- mittently through the Hawkesbury Sandstone, Wianamatta Group and their equivalents.

Genus GUTTATISPORITES Visscher 1966

Type species. Guttatisporites guttatus Visscher - original

des ignat ion.

Remarks.

Although Visscher (1966, p. 331) presented Guttatisporites as a verrucate genus, I employ an interpretation which encom passes a broader range of massive sculptural elements, the irregular outline and close spacing of these elements resulting in a negative reticulum.

Guttatisporites grandis sp. nov.

PI. 7 figs. 1-6

Description of specimens.

Microspores, radial, trilete. Amb circular to sub triangular.

Laesurae distinct, extend 1/2 to 2/3 radius, labrate (lips

1-1.5 microns wide, slightly riased. Exine 3-4 microns thick, exclusive of sculptural elements. Distal and proximal equa torial surface thickly set with heavy sculptural elements including baculae (3-7 microns long, 2.5 - 5 microns basal diameter) irregular verucae (2-4 microns high, 4-6 microns basal diameter) and abundant gemmate processes (up to 8 microns long,

6 microns basal diameter, 7 microns caput diameter constricted in central area 2-3 microns). Close spacing of sculptural ele ments results in negative reticulum in low focus. Size of sculptural elements diminishes approaching the apex, exine immediately adjacent to the laesurae is more or less smooth. - 96-

Dimensions .

Equatorial diameter 74 (94) 119 microns. 20 specimens

measured from sample 726.

Type locality.

Balmain Shaft at 1134 ft. (Bald Hill Claystone)

Ho 1o typ e .

Slide 726/2 48.0 999.4 Illustrations PI. 7 figs. 3, 5.

Remarks.

Specimens of Guttatisporites grandis are almost invariably

heavily carbonised. Sculptural elements occurring on single

specimen may be mixed or confined to a single style.

Comparisons.

Species previously assigned to Guttatisporites do not usually

display discrete, projecting sculptural elements.

Occurrence.

Guttatisporites grandis was first encountered in a basalmost Narrabeen Group microflora. It occurs intermittently

throughout the Narrabeen Group attaining maximum prominence in

the Bald Hill Claystone. It has not been identified with con

fidence above the Narrabeen Group.

Genus CONVERRUCOSISPORITES Potonie & Kremp 1954.

Type species. Converrueosisporites triquetrus (Ibrahim) Potonie

& Kremp - original designation.

Converrueosisporites eameroni (de Jersey) Playford & Dettmann.

Illustrations - See PI. 8

? 1953 Type 26A - Taylor, p. 159, p.160 fig. 26A.

1962 Verrueosisporites eameroni de Jersey, p. 6, pi. 2 figs. 2,3. - 97-

1965 Converruoosisporites oameroni (de Jersey) Playford &

Dettmann, p. 136, pi. 12 figs. 11-13.

Descriptions of specimens.

See de Jersey (1962, p. 6)

Remarks.

Type 26A, as illustrated by Taylor (1953, p. 160) is more closely allied to the concept of Lophotritetes novious Singh than of Converruoosisporites oameroni. However, as indicated by Playford & Dettmann (1965, p. 136) C. oameroni exhibits a wide range of sculptural diversity. At the other end of the range elements of the C. oameroni population are indisting uishable from specimens assigned to Neoraistriokia taylori

Playford & Dettmann. This, together with the duplicate ranges of these forms in most sequences, suggests that they are pro bably very closely related.

Previous Records.

Converruoosisporites oameroni Playford & Dettmann is re ported from both the Triassic and Early Jurassic strata of the

Leigh Creek Coal Measures (Playford & Dettmann, 1965). It also occurs in Ipswich Coal Measures of the Ipswich-Clarence Basin

(de Jersey, 1962). It is also recognised in the Moolayember

Formation, Clematis Sandstone and Wandoan Formation of the Surat

Basin.

Occurrence.

This species is first recognised in the Gosford Sub Group in the Sydney Basin. It extends throughout the Hawkesbury

Sandstone, Wianamatta Group and their equivalents. - 98-

Genus NEORAISTRICKIA Potonie 1956.

1949 Cepulina Malyavkhina (partim. ), p. 73

1956 Neoraistriokia Potonie p. 34

1959 Retioulatisporites ? Ibrahim, Krutzsch, p. 162

1964 Horriditriletes Bharadwaj & Salujha, p. 193.

Type species. Neoraistriokia trunoatus (Cookson) Potonie -

- original designation.

Remarks.

Dettmann (1963, p. 35) has discussed the synonymy of

Neoraistriokia and development of the generic concept. Bhara dwaj & Salujha (1964, p.193) proposed Horriditriletes to accommodate essentially identical forms to Neoraistriokia.

This distinction is obviously subjective and scarcely diag nostic at generic level.

Neoraistriokia ramosa (Balme & Hennelly) Hart

PI. 9 figs. 1, 5.

1952 P.27B Balme, p. 9 fig. 45.

1956b Aoanthotriletes ramosusBalme & Hennelly, p. 349, pi. 3

f igs. 39-41

1960 Neoraistriokia ramosus (Balme & Hennelly) Hart, p. 3, pi. 3

f ig . 39.

1964 Horriditriletes cf. H. ramosus (Balme & Hennelly) Bharadwaj

& Salujha, p. 194, pi. 2 fig. 43

Rema rks.

The sculptural elements of specimens which exhibit bifucat- ing baculae are usually shorter than the elements on specimens which display normal baculae. - 99-

Occurrence.

Neoraistrickia ramosa (Balme & Hennelly ) Hart is a rare component of Late Permian coal measure microfloras. It extends into basal zonule of the Protohaploxypinus retioulatus

Assemblage Zone.

Neoraistriokia pioketti sp. nov.

PI. 9 figs. 2-4, 6-12, 14, 15.

Description of specimens.

Microspores, trilete. Amb varying from circular to sub- triangular with full convex sides and rounded corners. Periphery interrupted by sculptural elements. Laesurae distinct, extending almost to periphery, accompanied by broad (1.5 microns wide), low (about 1 micron above general level) labrae. Exine not noticeably layered, 1.5 microns thick. Distal and equatorial surfaces bearing scattered discrete sculptural elements including baculae (up to 3 microns basal diameter, up to 6 microns in length), coni (2 microns basal diameter 2.5 microns high) and blunted spines (up to 4 microns in length 2-3 microns basal diameter). Baculae predominate and are often pilate or branched at lateral extremities. Contact face has much reduced sculptural elements in equatorial regions but is predominantly smooth or faintly scabrate.

Dimens ions.

Equatorial diameter 31 (39) 51 microns. 20 specimens measured.

(exclusive of sculptural elements.)

Type locality.

Camden 1 mile G.R. 664 811 (Picton Formation) - 100-

Holotype.

Slide 391/2 34.8 120.5 Illustrations - PI. 9 figs.4, 8, 12

Remarks.

Although the population includes specimens with circular

ambs the predominant shape of this species is rounded triangular

There also exists a wide range of variation in the size and

spacing of the sculptural elements.

Comparisons.

Neoraistrickia taylori Playford & Dettmann has a more dis

tinctly triangular amb, usually displays longer sculptural

elements, which are not predominantly thickened at the extre mities and has shorter, usually simple laesurae.

Occurrence.

Heoraistrickia picketti was first encountered in the central

portion of the Hawkesbury Sandstone. It extends through the

Wianamatta Group to the Picton Formation. It has also been

identified in the central and upper portions of the Wollar

Sandstone and its equivalents.

N eoraistrickia taylori Playford & Dettmann

Illustrations see Plate 8.

1953 Type 19B Taylor, p. 159, p. 160 fig. 19B.

1965 Neoraistriokia taylori Playford & Dettmann, p. 138, pi. 12

figs. 14, 15

Description of specimens.

Microspores, trilete. Amb variable, ranging from rounded triangular to distinctly triangular with concave sides and rounded apices. Distal surface bluntly conical in lateral view, - 101- proximal surface flatly pyramidal. Laesurae usually distinct, vary in length from 2/3 to almost full radius. Exine not noticeably layered, 1-1.5 microns thick, covered with scattered sculptural elements. Sculptural elements usually discrete, comprise baculae, coni and verrucae. Baculae up to 12 microns in length, 4 microns basal diameter, often branching. There is a distinct tendency for baculae to be most closely packed in the vicinity of the apices. Coni and verrucae up to 4 microns high, 3 microns basal diameter. Spacing of sculptural elements extremely variable. Size of elements much diminished on proximal surface, elements usually absent from the immediate vicinity of the laesurae.

Dimens ions .

Equatorial diameter 33 (45) 57 microns. 20 specimens

measured from sample 1005.

Polar diameter 35 - 49 microns.

Remarks.

Although Playford & Dettmann (1965, p. 138) specifically exclude the specimen drawn by Taylor (1953, p. 160 fig. 19B), forms of this general morphology are included in the populations assigned to Neoraistrickia taylori above. These populations are characterised by extreme variation in the size and dispo sition of sculptural elements, some end members of this range conforming to the concept of Converruoosisporites oameroni

(de Jersey) Playford & Dettmann.

Previous records.

Neoraistriokia taylori is reported from the Triassic and - 102-

Early Jurassic of the Leigh Creek Coal Measures (Playford &

Dettmann 1965, Table 1) the Brady Formation of northern Tas mania, from the Moolayember Formation (de Jersey & Hamilton,

1967) the Clematis Sandstone (de Jersey, 1968) and the Wandoan

Formation (de Jersey & Hamilton, 1969) of the Surat Basin. These occurrences are all regarded as Mid or Late Triassic in age.

Occurrence.

Neoraistriekia taylori first appears in the lower portion of the Narrabeen Group in the Sydney Basin. It extends through out the Hawkesbury Sandstone, Wianamatta Group and their equi valents .

Infraturma MURORNATI Potonie & Kremp 1954

Genus TIGRISPORITES Klaus 1960

Type species. Tigrisporites halleinis Klaus - original

des ignat ion.

Remarks.

Tigrisporites Klaus 1960 appears to be a potentially important biostratigraphic taxon. It has been reported from the Carnian of Austria (Klaus 1960), the upper Late Permian,

Loer and Middle Triassic of the Salt Range (Balme, 1969) and the Mid to Late Triassic of Australia (Playford 1965; de Jersey

& Hamilton 1967).

Playford (1965, p. 185) distinguishes Tigrisporites from the

Jurassic form Tripartina Malyavkhina 1953 ex. Potonie 1960 on the basis of the interradial sculpture of Tigrisporites. Sculp tural elements do not reach the equator in Tripartina. Balme

(1970, p. ) suggests that Tigrisporites can be distinguished from - 103-

Costaspora Staplin & Jansonius (in Staplin, 1960) by the distal verrucae and grana of the Mississipian form.

Tigrisporites play for di de Jersey & Hamilton 1967

PI. 10 figs. 1-3.

1965 Tigrisporites sp. Playford, P. 186, pi. 8 figs. 3, 4.

1967 Tigrisporites playfordi de Jersey & Hamilton, p. 10, pi. 5

f igs. 5-7.

1970 Tigrisporites catenatus Balme, p. , pi. 2 figs. 1, 2.

Description of specimen.

See de Jersey & Hamilton (1969, p. 10)

Dimens ions.

Diameter in polar view 28 (40) 49 microns. 20 specimens

measured.

Height in lateral view 28-38 microns.

Remarks.

The appearance of Tigrisporites playfordi in basal Narrabeen

Group microfloras constitutes an important biostratigraphic parallelism with its occurrence and first appearance in the

Chhidru Formation of the Salt Range (Balme, 1970).

Occurrence.

Tigrisporites playfordi first appears in basal Narrabeen

Group microfloras and occurs as a rare but constant component of the overlying Triassic microfloras. It is noticeably less prominent in microfloras containing Lunatisporites.

Genus CONVOLUTISPORA Hoffmeister et al. 1955

'Type species. Convoluti spora florida Hoffmeister et al. -

originai designation. - 104-

Convolutispora sp. 1

PI. 10 figs. 4, 5, 8-11.

Description of specimens.

Microspore, radial, trilete. Amb circular to rounded sub- triangular with dentate periphery due to projecting sculptural elements. Laesurae straight, simple, extend about 3/4 radius, often difficult to detect. Exine not noticeably layered, more or less covered with broad (3-6 microns wide), flat (2-3 microns high) often anastomosing rugulae which are interspersed with and surmounted by massive coni, cristae and irregular verrucae (basal diameter up to 8 microns, may project 8 microns above level of rugulae). Sculpture diminishes in intensity approaching the laesurae.

D imens ion s.

Equatorial diameter 54 (67) 90 microns. 15 specimens

(exclusive of sculptural elements) measured.

Remarks.

Convolutispora sp. embraces specimens displaying a consider able variation in the development of the projecting sculptural elements. The range of this variation is illustrated on plate 10.

Comparisons.

Convolutispora florida Hoffmeister et al. has shorter, lipped laesurae; lacks the large projecting sculptural elements and has a smaller mean size. Retioulatisporites horribilis sp. nov. is distinguished by its finer, distinctly reticulate basic sculp ture pattern.

Occurrence.

Convolutispora sp. 1 is first encountered in the Newport - 105-

Formation of the Narrabeen Group. It extends throughout the

Hawkesbury Sandstone, Wianamatta Group and their equivalents.

It is invariably a rare component of the microfloras in which

it occurs.

Genus FOVEOSPORITES Balme 1967

Type species. Foveosporites oanalis Balme - original designation

Foveosporites sp. cf. F. moretonensis de Jersey

PI. 10 figs. 6, 7; pi. 11 figs. 11,12; pi.12 figs. 7, 8.

1962 Foveosporites moretonensis de Jersey, p. 7, pi. 1 figs. 7, 8

Description of specimens.

Microspores, radial trilete. Amb circular, sub-circular or

rounded triangular. Laesurae seldom distinct, simple, straight,

extending half to two thirds radius. Exine not noticeably

layered, 2 - 4 microns thick. Distal and equatorial exine

foveolate to foveolate-reticulate. Pits have irregular shape

(0.5 - 6 microns diameter, 1 - 3 microns average) up to 2 microns

thick, usually closely spaced (seldom more than 6 microns apart,

2-3 microns average). Pitting reduced or absent on contact face.

Dimens ions.

Equatorial diameter 34 (52) 65 microns. 20 specimens

measured.

Remarks.

The majority of specimens assigned to Foveosporites sp. cf.

F. moretonensis are heavily carbonised despite clearing of the

exines of the remainder of the population. A large number were

also torn. The Sydney Basin population substantially exceeds the

size range of the Ipswich material as reported by de Jersey (28 - - 106-

38 microns). The thickened lips which de Jersey describes

were not encountered, although it must be confessed that

laesurae, as such, were recognised on only three specimens.

Comparisons.

Foveosporites pellucidus Playford & Helby from the Mid

Caboniferous Italia Road Formation (Playford & Helby, 1968)

has slightly longer laesurae, usually displays a more regular

foveolate pattern and a slightly larger mean size and size

range. These forms are very similar and is not improbable

that the Italia Road Formation and its equivalents intermit

tently contributed to sedimentation during deposition of the

Wianamatta Group. Foveosporites mimosae de Jersey & Hamilton

has smaller, more regular pitting of the exine.

Previous records.

Foveosporites moretonensis has only been recorded from the

Bundamba Group of south-eastern Queensland. Unidentified

species of Foveosporites are, however, relatively consistent

in microfloras of the Moolayember Formation and Wandoan Form

ation of southern Queensland (de Jersey & Hamilton, 1967, 1969).

Occurrence.

Foveosporites sp. cf. F. moretonensis was first encountered

in the lower portion of the Hawkesbury Sandstone and extended

to at least the Annan Shale of the Wianamatta Group.

Genus MICROFOVEOLATISPORA Bharadwaj 1962

Type species. Microfoveolatispora raniganjensis Bharadwaj -

original designation.

Microfoveolatispora raniganjensis Bharadwaj PI.11 figs .9,13,15 . - 107-

1962 Microfoveolatispora raniganjensis Bharadwaj, p. 82, pi. 2

figs. 48, 49.

Description of specimens.

see Bharadwaj 1962, p. 82.

Dimens ions.

Equatorial diameter 48 (63) 78 microns - 20 specimens

measured from sample 981.

Remarks.

Microfoveolatispora raniganj ensis Bharadwaj is a distinc

tive form. All specimens encountered appeared overmacerated,

although other species in the same sample were relatively well

preserved.

Occurrence.

Microfoveolatispora raniganj ensis was encountered only in

sample 981 from the Vales Point Coal Member.

Genus DICTYOTRILETES Naumova emend. Potonie & Kremp 1954.

Type species. Dictyotriletes bireticulatus (Ibrahim) Potonie

& Kremp - designated by Potonie & Kremp (1954,

p . 144) .

Remarks.

Smith & Butterworth (1967, p. 194) proposed broadening the concept of Dictyotriletes to include forms previously assigned

to Reticulatisporites Ibrahim, but excluded from this genus by the emendation of Neves (1964). There exists considerable doubt concerning the validity of Neves’ interpretation of Reticulati sporites reticulatus Ibrahim as a cingulate form. As Neves evidence for the cingulum in R. reticulatus is scarcely con- - 108 - clusive, it is difficult to accept his emendation of the genus and thus the proposed emendation of Dicty otrilete s (Smith &

Butterworth, 1964) is not warranted. Reticulitriletes Maedler

1964 is regarded as a junior synonym of Dictyotriletes.

Dictyotriletes playfordi sp. nov.

PI. 11 figs. 1-5.

Description of specimens. Microspores, trilete, Amb more or less circular. Laesurae indistinct, sinuous, accompanied by narrow slightly raised labrae, extending 2/3 to 3/4 radius. Exine not noticeably layered, bearing very irregular reticulum on both distal and proximal surfaces. 1 micron wide, rounded 0.5 - 1 micron high; lumens up to 6 microns high; lumens up to 6 microns maximum diameter, shape irregularly polygonal. Exine 1 micron thick. Dimens ions. Equatorial diameter 34 (49.5) 60 microns. 25 specimens measured from sample 726.

Type locality. Balmain Shaft, dark grey shale at 1,134 ft. Holo typ e. Slide 726/2 6.5 112.3. Illustrations - PI. 11 figs. 1, 2. Remarks.

Although Dictyotriletes playfordi was only encountered in sample 726 it is a distinctive form and warrants formal des cription .

Comparisons.

Dicty otriletes densoreticulatus Potonie & Kremp is super ficially similar but has considerably broader muri which appears - 109- to bear slight projections at junction with other muri, more regular lumens and a larger mean size (60-80 microns - size range). Dictyotriletes reticulocingulum (Loose) Smith & Butter- worth has a well developed reticulum on the distal surface only, with more massive muri. Dictyotriletes globosus (Maedler) comb, nov. (Reticulitriletes globosus Maedler, 1964, p. 76, pi. 5 figs. 8, 9) has smaller, regular lumens. Dictyotriletes sp. illustrated by Hoeg & Bose (pi. 34 fig. 6) is superficially s imilar. Occurrence.

This species has only been recognised in a single sample form the Bald Hill Claystone.

Reticulatisiporites magnidictyus Playford & Helby. PI. 9 fig. 13. 1968 Reticulatisporites magnidictyus Playford & Helby, p. 110, pi. 10, f igs. 7-10. Desription of specimens. See Playford & Helby (1968, p. 110). Remarks. The specimens assigned to Reticulatisporites magnidictyus Playford & Helby are indistinguishable from the Carboniferous population described by those authors (1968 pp. 110-111). The presence of other diagnostic components of the Grandispora micro flora (Helby, 1969) suggests that these specimens are probably recycled from Carboniferous source areas to the immediate north of the sample location. Occurrence.

A number of specimens were encountered in sample 991, between - 110-

the Vales Point Coal Member and the Wallarah Seam, in

Newvale D.D.H. No. 28.

Retioulatbsporites horribilis sp. nov.

PI. 11 figs. 7, 8, 10 14.

Description of specimens.

Microspore, radial, trilete. Amb circular, periphery

interrupted by projecting sculptural elements. Laesurae

seldom distinct, extend almost full radius, usually straight.

Exine not noticeably layered. Proximal and distal surface

covered with reticulate sculptural pattern. Shape of lumens

irregular polygonal, ranging from 3-6 microns maximum diameter.

Muri irregular, usually about 2 microns thick, upper surface

irregular often surmounted by irregular spines and cristae,

up to 5 microns above general level of muri. Projections occur mainly at the junctions of the muri. Sculpture diminishes

slightly approaching the laesurae.

Dimens ions.

Equatorial diameter 55 (61) 70 microns. 10 specimens measured, (exclusive of sculpture).

Type locality.

Wollongong D.D.H. No. 28 184 ft. - Upper portion of the

Hawkesbury sandstone.

Holotype.

Slide 521/1 36.0 115.0 Illustrations - PI. 11 figs. 10,

14. (size 66 microns).

Remarks.

Despite the irregularities of lumen shape, the basic - 111-

sculpture pattern of this species is reticulate.

Comparisons.

Diotyotritetes densoretioulatus Potonie & Kremp, has more

regularly shaped lumens and thinner muri which lack projecting

elements. Retioulatispovites magnidiotyus Playford & Helby has much larger, distinctly polygonal lumens on the distal

surface and characteristically elongate lumens on the proximal surface. Convolutispora sp. 1 is superficially similar, but close examination reveals that the basic sculptural elements are generally discontinuous rugulae, rather than a reticulum.

Occurrence.

Reticulatispovites horribilis sp. nov. first appears in the

Hawkesbury Sandstone and extends through the Wianamatta Group and their equivalents.

Genus LYCOPODIUMSPORITES Thiergart ex Delcourt & Sprumont 1955

Type species. Lyoopodiumsporites agathoeous (Potonie) Delcourt

& Sprumont - selected by Delcourt & Sprumont

(1955, p. 31)

Selected Synonymy.

1934 Sporites (partim.)3 Potonie, p. 43, pi. 1 fig. 25.

1938 Lyoopodium-sporites Thiergart, p. 293, pi. 22.

1955 Lyoopodiumspovites Thiergart ex Delcourt & Sprumont, p. 31.

Remarks.

Delcourt & Sprumont (1955 pp. 31, 32) presented a generic diagnosis of Lyeopodiumsporites and selected L. agathoeous

(Potonie) Delcourt & Sprumont as type species, thereby validating the genus. Krutzsch (1959, p. 159) maintains that the illus- - 112- trations which Thiergart (1938, pi. 22 figs. 9. 10) presented as Lycopodium-spovites aff. agathoeous Potonie are morpho logically distinct from the form described by Potonie (1934, pi. 1 fig. 25) as Spovites agathoeous. On this basis he insists that the genus Lyoopodiumspovites is invalid, sug gesting that the concept of the genus as envisaged by Thiergart could be included in the previously validated genus Micvo- vetioulatispovites Knox ex Potonie & Kremp 1954. It is apparent that Krutzsch has overlooked the full implications of Delcourt & Sprumont’s validation of Lycopodiumspovites by selecting L. agathoeous as type species. This oversight is further complicated by Krutzsch's recombination of Spovites agathoeous Potonie with Foveospovis Krutzsch 1959.

However, it remains that Ly copodiumspovites is yet to be

satisfactorily delineated from a number of form genera inclu ding Retioulatispovites Ibrahim emend. Potonie & Kremp 1954 and Miovovetioulatispovites Knox ex Potonie & Kremp 1954.

Lycopodiumspovites sp. cf. L. vetioulumsporites (Rouse) Dettmann

PI. 12 figs. 1-3

1959 Lycopodium vetioulumsporites (pavtim.) Rouse, p. 309, pi. 2

f igs . 1, 2.

1963 Ly copodiumspovites vetioulumsporites (Rouse) Dettmann,

p. 45, pi. 7 figs.4-7.

Description of specimens.

Microspores, radial, trilete. Amb sub circular to convex triangular with well rounded corners. Laesurae distinct; usually accompanied by thin, slightly raised membranous lips; extend - 113-

about 3/4 radius, more or less straight. Exine not noticeably

layered, displaying reticulum on proximal and distal surfaces,

lumens 2-6 microns diameter with polygonal outline, muri 0.5-1

micron wide, 1-1.5 microns high.

Dimens ions.

Equatorial diameter 26 (34) 45 microns. 7 specimens

measured .

Remarks.

Specimens assigned to this category conform fairly closely

to Lyoopodiumsporites reticulumsporites although the elongation

of the lumens on the proximal surface was not noted.

Occurrences.

A single specimen of Lyoopodiumsporites sp. cf. L. reti- outumsporites was identified from the central portion of the

Hawkesbury Sandstone. It occurs intermittently as a rare component of microfloras of the Wianamatta Group.

Genus INDOSPORA Bharadwaj 1962.

Type species. Indospora o'Lara Bharadwaj - original designation.

Remarks.

I regard the presence of a distal reticulum, often sur mounting a slight distal crassitude which may extend into triradiate thickenings represented at the apicies as auricular projections, as the significant diagnostic feature of the genus

Indospora Bharadwaj 1962.

Indospora olara Bharadwaj 1962.

PI. 12 figs. 4-6, 9-12, 14-17. - 114-

Synonymy .

Indospora clara Bharadwaj 1962, p. 83, pi. 3, figs. 54, 55.

Indospora macula Bharadwaj & Salujha 1964, p. 195, pi. 2,

f igs. 54 , 56.

Indospora reticulata de Jersey 1968, p. 9, pi. 2, figs.1,2,4,5.

Description of specimens.

Amb triangular, sides varying from slightly concave to

markedly convex. Apicies often rounded. Trilete, laesurae

usually extending almost to periphery. Exine about 2 microns

thick, displaying a distal crassitude which is covered by a

coarse (lumens 4-7 microns, muri 1-3 microns wide, 1-2 microns

high, usually imperfect reticulum. The limits of the distal

crassitude are roughly parallel to the sides of the spore, but

often extend to the apicies as narrow, radial strips, thickening

at the periphery to form auriculae (PI. 12 figs. 9 and 12).

Remainder of distal surface covered with scattered sculptural

elements including coni, spines, verrucae, baculae and low,

thick, often radially orientated rugulae.

Coni - basal diameter 1-3 microns height 1-3 microns.

Spines " " 1-3 " " 3-5

Verrucae " " 2-3 " " 1-3

Baculae " " 2-3 " " 2-8

Dimens ions.

36 (46) 58 microns. 25 specimens measured.

Remarks.

The specimens described above conform essentially to

the original concept of Indospora clara Bharadwaj 1962, al

though it could be argued that a rather broad interpretation - 115- has been made. Bharadwaj and Salujha (1965) attempted to delineate X. macula from X. clara on the basis of its finer sculptural elements and better developed reticulum. On similar basis de Jersey (1968, p. 19) has proposed X. reticulata. However, the forms encountered in this study show a complete gradation of sculptural elements and marked variation and development of the distal reticulum.

Previous records.

Indospora clava has previously been reported from the

Upper Permian Raniganj Stage, (Bharadwaj & Salujha,1965) India and the Chhidru Formation of the Salt Range (Balme,1970). It is also noted in the Upper Permian Wagina Sandstone of the Perth Basin, Western Australia. I have also encountered this form in samples of Kockatea Shale (basal Triassic - supplied by Dr. B.E. Balme) and de Jersey (1967) indicates that it extends from the uppermost Rewan Formation through the Clematis Sandstone. Occurrence. Indospora clara is encountered intermittently throughout the Narrabeen Group, Hawkesbury Sandstone and Wianamatta Group. It is relatively common in the basal Narrabeen Group and the Hawkesbury Sandstone and its equivalents. Genus DULHUNTYISPORA Potonie 1956.

Type species. Dulhuntyispora dulhuntyi Potonie - original des ignat ion. Lectotype assigned by Potonie (1956) from

Dulhunty 1946, pi. 7 fig* 2lA. - 116-

Synonymy .

1956 (September) Dulhuntyispora Potonie, p. 37, pi. 4 fig. 38.

1956b (October) Tholosporites Balme & Hennelly, p. 254.

Remarks.

Dulhuntyispora Potonie 1960 appears to be confined to

Mid to Late Permian sediments of Australia. As such it is

an important biostratigraphic indicator. Balme (1964) has

commented on the ubiquity of its appearance in the Australian

Late Permian, delineating a Dulhuntyispora Assemblage. Evans

(1970) uses the first appearance of D. parvithola (Balme &

Hennelly) to delineate the base of his Late Permian Stage 5.

Paten (pers. eomm.) suggests that D. dulhuntyi Potonie 1956

appears earlier than D. parvithola.

Jansonius (1962) tentatively assigned a form, D . ? minuta

to this genus. However, the interradial ornamentation of this

form is definitely not inflated like the typical "scutula" of

Dulhuntyisporaj and the Canadian specimens all bear an annular distal crassitude. The general organisation is somewhat similar to Simeonospora Balme 1970 although Simeonospora does not display a distal crassitude.

Dulhuntyispora dulhuntyi Potonie 1956

PI. 12 fig. 13

1946 21A Dulhunty, p. 155, text fig. 2-21A, pi. 7 fig. 21A.

1952 P21A (Dulhunty). Balme, p. 9, text fig. 45-21A.

1956 (Sept.) Dulhuntyispora dulhuntyi Potonie, p. 37, pi. 4

fig. 38.

1956b (Oct.) Tholosporites egregius Balme & Hennelly, p. 254,

pi. & figs. 12-lb. - 117- Remarks .

In New South Wales D. dulhuntyi is a rare but persistant component of Late Permian coal measure microfloras. It's oldest occurrence in the Sydney area to date is in the upper part of the Wandrawadrian Sandstone to the immediate south of Sydney.

Occurrence.

In the present study D. dulhuntyi was encountered as poorly preserved, broken specimens in basal Narrabeen Group microfloras in Terrigal No. 1 well and in the Cox’s Gap outcrop s ection.

Dulhuntyispora parvithola (Balme & Hennelly) Potonie PI. 13 figs. 13-16

1956b Tholosporites parvitholus Balme & Hennelly, p. 255 , pi.10

figs. 76-80. 1956 Dulhuntyispora parvithola (Balme & Hennelly) Potonie p. 44. Description of specimens. See Balme & Hennelly 1956b, p. 255. D imens ions.

Diameter 42 (62) 85 microns. 25 specimens measured. Remarks.

As mentioned by Balme & Hennelly (1956b, p. 255) the inflation of the "scutulae" or interradial blisters on the proximal faces of the specimens is not a constant feature.

In some specimens the scutulae have ruptured and it is possible to detect a thin intexine. D. parvithola is relatively common in New South Wales Late Permian microfloras. Evans (1966) - 118- reports its occurrence in basal Narrabeen Group and Lower

Rewan Formation microfloras.

Occurrence.

In the present study D. parvithola was present in all

Newcastle Coal Measure samples. It is relatively common in all basal Narrabeen Group microfloras and is virtually absent towards the top of the Lunatisporite s pellucidus Assemblage

Zone.

Genus LESCHIKISPORIS Potonie 1958.

Type species. Leschikisporis aduncus (Leschik) Potonie -

- original designation.

Selected Synonymy.

1950 Punctatisporites (Ibrahim) Schopf, Wilson & Bentall

(partim.) Kosanke, p.16, pi. 2 fig. 5

1955 Punctatisporites Ibrahim (partim.) Leschik, p. 27, pi. 3

figs. 16. 17.

1966 Circlettisporites Miller, p. 224, pi. 1 figs. 1-12

Remarks.

Potonie (1958, p.18) proposed the genus Leschikisporis to encompass microspores with an assymetrical trilete mark and a smooth to granulate exine. This assymetry is manifested by a shorter ray, joining two other rays which may be arranged in rough alignment. Microspores of this organisation have been extracted from fertile remains of Asterotheca meriana

(Brongniart) Star by Bharadwaj & Singh (1956, pi. 2 figs. 12,21).

The relationship of these spores to Leschikisporis aduncus

(Leschik) Potonie was pointed out by Maedler (1964, p. 103). - 119-

Bharadwaj & Singh (1956) and Potonie (1962) had previously

compared the spores of A. meviana to the monolete genus

Latospovites Potonie & Kremp 1954. Bharadwaj & Singh (1964,

p. 35) also drew attention to the similarity of A. meviana

microspores and L. aduncus. These authors proposed an

emendation of the genus Leschikispovis based on their inter

pretation of laesurate organisation of L. aduncus as monolete,

transferring the genus to the Sculptomonoleti. In view of the

obvious ambivalent nature of the laesurate geometry, and the

wide range of variation of this character displayed (see

Maedler, 1964, pi. 9 figs. 4-7) by the type species there is

little purpose to be served by suprageneric shuffling.

Microspores referable to Leschikispovis have been

described by Kosanke (1950) as Punctatispovites obliquus

and Peppers (1964) as Punctatisporites saetigev from

Pennsylvannian strata of the Illinois Basin, U.S.A.

I employ a somewhat broader concept of Leschikispovis

than that outlined by Potonie (1958) or Bharadwaj & Singh

(1964), in that it is expanded to included forms which may

display both verrucate, foveolate and foveo-reticulate exines.

Leschikispovis mutabilis (Balme) comb. nov.

PI. 13 figs. 1-12, 17-19.

1970 Polypodiispovites mutabilis Balme, p. , pi. 6 figs.7-9.

Description of specimens.

Microspores with asymetrical trilete scar. Amb circular

to oval, periphery usually irregular. Laesurae extremely variable, ranging from normal trilete to indisputable monolete. - 120-

Specimens with finer varieties of sculpture often display

low irregular, sculptured labrae accompanying the laesurae.

Exine 1.5 - 3 microns thick, sculptured proximally and distally with fine grana (0.5 - 1 micron, closely packed) verrucae and

or irregular rugulae (1-2 microns high) separated by sinuous

channels. Anastomosing of irregular rugulate elements variable,

resulting in pseudofoveolate of pattern or negative reticulum.

Dimensions.

Maximum diameter 24 (34) 56 microns. 25 specimens

measured from sample 978.

Maximum diameter 26 (38) 56 microns. 25 specimens

measured from sample 530.

Specimens were measured by traverse, every specimen inter sected by cross hairs was measured.

Remarks.

Although Balme (1970) did not stress the variability of the species, Lesohikisporis mutabilis affords a remarkable example of the range of gradational, morphological diversity which microspore species may exhibit. The degree of asymmetry of the laesurate geometry appears to be directly related to the eccentricity of the outline of the grain. Sculptural patterns are usually constant on both surfaces of individual grains.

There is no relationship between size of grain and sculptural pattern, suggesting that variation of sculptural pattern is probably not related to the maturity of the spores prior to release from the sporangia.

Previous records.

Lesohikispovis mutabilis is recorded as a rare to common - 121- component of Late Permian microfloras extracted from the

Chhidru Formation of Pakistan (Balme, 1970).

Occurrence.

Leschikisporis mutabilis occurs intermittently throughout the Narrabeen Group and the Hawkesbury Sandstone. It locally dominates microfloras in the lower portion of the Gosford

Sub-Group.

Subturma ZONOTRILETES Waltz 1935

Genus DUPLEXISPORITES Deak emend. Playford & Dettmann 1965

Type species. Duplexisporites generalis Deak - original

designation.

Remarks.

In emending Duplex-ispovites Playford & Dettmann (1965 , p. 140) interpreted the genus as acingulate. However, par ticularly in the case of D. problematicus (Couper) Playford

& Dettmann I consider the "interradial muri" to be continuous and also located at the equator, (see Couper 1958, pi. 24 fig. 12, 13 and also this volume, pi. 15 fig. 19) As such, this structure is interpreted as a cingulum. The diagnosis stated by those authors is otherwise accepted.

Duplexisporites problematicus (Couper) Playford & Dettmann

PI. 15 figs. 15,16,18-20.

Selected Synonymy.

1958 Cingulatisporites problematicus Couper, p. 146, pi. 24

figs. 11-13.

? 1960 Periplectotriletes amplectus (Waltz) var. taimyrensis

Kara Murza, pi. 9, fig. 5. - 122-

? 1962 Azonotriletes interextus (Naumova) var. triassioa

Kara Murza, Tschalyschev & Varyukhina, pi. 5, fig. 10.

1965 Duplexisporites problematious (Couper) Playford & Dettmann

p . 140 .

1965 Duplexisporites gyratus Playford & Dettmann, p. 141.

pi.13 figs. 20-22

1965 Contignisporites problematious (Couper) Doring, p. 51,

p i . 18 figs. 6-8.

Description of specimens.

Microspores, trilete, cingulate. Amb convex sub-trian

gular to sub-circular. Laesurae distinct, extend about 2/3

radius, sometimes accompanied by slightly raised lips. Exine not obviously layered, about 2 microns thick. Cingulum 2-4 microns wide, slightly broader in interradial regions. Distal

surface mostly covered by low (2-3 microns high), rounded but broad (2-6 microns wide) exinal thickening or ridge (murus).

This ridge is disposed in a sub-triangular spiral, the sides of which are more or less parallel to the sides of the spores but may have been displaced by deflation of the distal hemi sphere. Equatorial end of the ridge joins the cingulum, usually at a corner. In most specimens the ridge is continuous for the first spiral but often breaks up into large randomly placed rugulae and verrucae approaching the distal pole. Dis tance between sculptural elements extremely variable (0.5 - 3 microns). Exine between and comprising sculptural elements is laevigate to punctate. Exine of proximal surface is laevigate.

Dimensions.

Diameter. 37 (44) 72 microns. 15 specimens measured. - 123-

Remarks .

Playford & Dettmann (1965) suggest that Duplexisporites gyratus Playford & Dettmann can be distinguished from D. problematious (Couper) Playford & Dettmann by the wide gap between the ridge spirals and the undulating surface of the

ridges in the latter form. The assemblage described above

encompasses a broad but continuous morphological range which would include both species. As D. problematious has obvious priority D. gyratus is assigned to synonymy.

Previous records.

In south-eastern Queensland Duplexisporites problematious extends from Mid to Late Triassic (Moolayember Formation - de Jersey & Hamilton 1967) into probable Mid Jurassic

(Precipice Sandstone and Evergreen Shale - de Jersey & Paten

1964). It is reported ranging through a sedimentary section at

Leigh Creek South Australia, to which Playford & Dettmann (1965) assign a Rhaetic-Liassic age. Playford (1965) has identified this form from a probable equivalent of the Brady Formation in north-eastern Tasmania.

Comparisons.

Duplexisporites problematious is distinguished from

D. soanious (Nilsson) Playford & Dettmann by the irregular width and shape of the sculptural ridge of the latter form.

It is distinguished from D. generalis Deak in having rugulae and verrucae in the vicinity of the distal pole.

Occurrence.

In the present study D. problematious first appeared - 124-

in the central portions of the Hawkesbury Sandstone and its

equivalents. It ranges through the Wianamatta Group as a

rare but persistent component of the microflora.

Genus CONTIGNISPORITES Dettmann 1963

Type species. Contignisporites glebulentus Dettmann - original

designation.

? Contignisporites Sydneyensis sp. nov.

PI. 14 figs. 5-12.

Description of specimens.

Microspores, trilete, cingulate. Amb rounded triangular

to sub-circular. Laesurae distinct, extend to inner edge of

the cingulum accompanied by slightly raised lips. Folds often

develop along the laesurae. Exine not noticeably layered,

1-1.5 microns thick on proximal surface. Distal surface

exhibits low (1-2 microns), broad (2-4 microns), often sinuous

ridges which form an irregular reticulate pattern. Equato-

rially these ridges merge with the cingulum. Cingulum up to

8 microns wide, uniform in width, although extending onto

proximal surface at the termini of the laesurae to form

perfect curvature. Contact faces laevigate.

Dimensions.

Equatorial diameter 60 (66) 76 microns. 10 specimens

measured from sample 522.

Type locality.

Wollongong D.D.H.No. 28 at 242 ft. (Hawkesbury Sandstone)

Holotype.

Slide 522/1 31.3 102.5 Illustrations - PI. 14 figs.8, 9.

(68 microns) - 125-

Remarks .

As defined by Dettmann (1963, p. 73) the form genus

Contignispovites accommodates trilete cingulate, microspores

with broad, more or less parallel but often anastomosing massive

ridges on the distal surface and a sub-equatorial murus on each

contact face. Although ? Contignispovites Sydneyensis sp. nov.

lacks the interradial muri which characterise Contignispovites

and has a distinct distal reticulate pattern the overall organi

sation most closely resembles this genus. The spiral disposition

of the distal sculpture of dupiexispovites Deak emend. Playford

& Dettmann 1965 eliminates that form as an appropriate genus.

In emending Retioulatispovites Ibrahim 1933, Neves (1964) re

interpreted the type species as having a cingulate organisation.

Contrary views have been expressed by Potonie (1966), Doubinger

& Rauscher (1966) and Playford & Helby (1968). Despite possible

acceptance of Neves interpretation the nature of the reticulum

of ? C. Sydneyensis more closely resembles Diotyotvitetes

Naumova emend. Potonie & Kremp 1954.

Comparisons.

Duplexispovite s pvob'Lematicus Couper occurring in the same

samples as ? Contignispovites sydneyensis sp. nov. is readily distinguished by the spiral nature of the distal sculpture.

Contignispovites glebuientus Dettmann, C. eooksonii (Balme)

Dettmann, C. fovnieatus Dettmann and C . muttimuvatus Dettmann all display interradial sculpture.

Occurr ence.

This form is first encountered in the upper portion of the

Hawkesbury Sandstone and extends into the Picton Formation of the - 126-

Wianamatta Group. It invariably occurs as a rare or very minor component of the microflora.

Genus TRIPARTITES Schemel 1950

Type species. Tripartites vestatus Schemel - original

des ignation.

Remarks.

Potonie (1956, p. 55) and Potonie & Kremp (1956, p.91) indicate that Tripartites Schemel 1950 was emended by Potonie

& Kremp (1954). However, there is no record of this genus being emended in Potonie & Kremp (1954, p. 154), although the form is discussed at length. This oversight has been perpetuated in the literature.

Staplin (1960, p. 26) drew attention to the presence of two, possibly mutually overlapping, morphological groups in forms which have been assigned to Tripartites Schemel. Group A included forms which do not exhibit a continuous equatorial girdle. Group

B included forms exhibiting a continuous equatorial girdle. It is noted that the type species Tripartites vestatus Schemel 1950 could be assigned to Group A.

I regard the presence of plications in the radial crassi tudes (auriculae) as the diagnostic feature distinguishing

Tripartites of Group A from Triquitrites Wilson & Coe 1940 emend.

Potonie & Kremp 1954.

Tripartites proratus (Balme) comb. nov.

PI. 15 figs. 7-9

1970 Triquitrites proratus Balme, p. , pi. 3, figs. 6-8. - 127-

Description of specimens.

Microspores, trilete, auriculate. Amb triangular, sides distinctly concave. Laesurae distinct, extending almost to the inner edge of auriculae, lips not apparent, but folds sub-parallel to the laesurae are relatively common. Exine not noticeably layered, 1-2 microns thick (except at auriculae), laevigate to finely granulate. Auriculae confined to corners, with no sign of an interradial crassitude or "girdle". Auriculae 3-8 microns wide (measured radially) up to 22 microns maximum diameter. Outer edge of auriculae indented by 3-5 radial plications, lateral extremities elongated and in well preserved specimens (PI. 15 fig. 8). These curve in towards the spore body. In other specimens they are preserved as small spurs (PI. 15 fig. 7). Inner margin of auriculae markedly concave.

D imens ions.

Diameter 33 (37.5) 41 microns - 21 specimens measured.

Remarks.

Tvipartites proratus has been reported as a rare component of the Upper Permian Chhidru Formation of the Salt Range (Balme

1970) .

Occurr ence.

This form is encountered as a relatively rare but constant component of basal Narrabeen Group microfloras throughout the

Sydney Basin.

Forms with distal circumpolar differentiation.

Uppermost Permian and Triassic microfloras of the Sydney

Basin include an abundance of microspores which are characterised - 128- by distal, circumpolar exine elements and or polar crassitudes.

Most of these species are often characterised by the inconsis tent occurrence of these features. Valid genera to which species of this general organisation have been assigned include :

Cingulate forms Acingulate forms

Essentially smooth Roly cingulatisporites Annulispora

exine Duplexisporites Stereisporites

Sculptured exine Tauroousporites Ratti g anispora

Nevesisporites

All the above genera, apart from Nevesisporites de Jersey

& Paten 1964, were proposed to accommodate forms with distal circumpolar and or polar crassitudinous elements. As defined by de Jersey & Paten (1964, p. 8) Nevesisporites was erected to include cingulate microspores with sculptural elements confined to the contact faces. However, Playford (1965) employed a very much wider interpretation of the genus, assigning to it a species

(N. limatulus Playford) essentially similar to Nevesisporites but characterised by a distal polar crassitude. Playford (1965, p.188) noted the inconsistent occurrence of this feature. In

Sydney Basin populations of this species forms displaying the distal crassitude are overwhelmingly predominant. Balme, (1970), following Playford’s interpretation of Nevesisporites has assigned a further species (N. fossulatus). This form is essentially patinate with a distal circumpolar incision and thus the organi sation is more or less analogous to that of N. timatuius Play ford 1965. I consider that the organisation of these species is sufficiently diagnostic to warrant their removal from - 129-

Nevesispovites. As they do not conform to the concept of the other genera listed above, a new genus, Limatulaspovites, is proposed.

Genus LIMATULASPORITES nov.

Type species. Limatulaspovites limatulus(Playford)comb. nov.

- original designation.

Diagnos is.

Microspores, trilete. Amb circular to sub-triangular.

Distal surface bearing a circumpolar ring of thin exine which may be interpreted as the area between a cingulum and a polar crassitude or alternatively a circumpolar incision in a patina.

Distal exine surface more or less smooth, proximal surface may bear sculptural elements such as grana.

Comparisons.

Limatulaspovites gen. nov. differs from Poly oingulatispo- vites Simoncsics & Kedves emend. Playford & Dettmann 1965 in lacking a distinct, thickened, circumpolar ridge surrounding the distal polar crassitude. It differs similarly from

Tauvoouspovites Stover emend. Playford & Dettmann 1965.

AnnuZispova de Jersey 1959 possesses a distal, circumpolar, thickened ridge and appears to lack a cingulum. Steveispovite s

Pflug 1953 displays an intermittent, distal, polar crassitude, but lacks a distinct cingulum, although there is a slight tendency to develop equatorial interradial crassitudes.

Limatulaspovites bvunkevi sp. nov.

PI. 14 figs. 1 - 5

Selected Synonymy.

1960 Euvyzonotviletes miovodisous (K.M.), Tschalyschev & - 130-

Varyukhina, pi. 5 fig. 28.

? 1964 Seftenbergiites, Malyavkhina3 pi. 14 figs. 22, 23.

Description of specimen.

Microspores, trilete, patinate and cingulate. Amb circular to sub-circular, outline slightly irregular. Laesurae distinct, straight, extending almost to the equator. Laesurae fringed by low (1 micron high), broad (1-2 microns wide) labrae.

Distal and equatorial exine patinate (2-3 microns thick) deeply incised by a single, distal, circumpolar ring of thinner exine,

(0.5 - 2 microns wide). Surface of patina gently undulating.

Cingulum 2-3 microns wide, irregular in outline. Proximal surface smooth.

Dimens ions.

22 (28) 33 microns. 10 specimens measured from sample 555

30 (32) 35 microns. 10 specimens measured from sample 557

Ho lo ty pe.

Slide 555/2 25.4 120.5 PI. 14 figs. 1,2 (size - 27 microns)

Compar i sons.

Limatulasporites brunkeri sp. nov. is similar to Polyeingu- latisporites dejerseyi sp. nov., having an essentially patinate exine and characteristic broad labrae. However, it has only a single, distal circumpolar incision, a narrow wavy cingulum and a smaller, restricted size range. It differs from Limatula sporites sp. in possessing a cingulum, having a thicker patina and broad labrae.

R e m a r k s .

The similarities of Limatulasporites brunkeri sp. nov. and - 131-

Polyoingulatisporites deg erseyi sp. nov. are striking. I

believe that these forms are possibly microspore variants of

the same parent plant.

Occurrence.

The occurrence of Limatulasporites brunkeri is apparently

restricted to the Patonga Claystone in Ourimbah Creek D.D.H.

No . 5 .

Limatulasporites fossulatus (Balme) comb. nov.

PI. 15 figs. 1-6.

Selected Synonymy.

? 1956 Leiotriletes furoatus Bolkhovitina, p. 36, pi. 3 fig. 2

1962 Leiotriletes arquatus (Portn.) Naum., Tschalyschev &

Varyukhina, pi. 5 fig. 11.

? 1964 Selaginella rarirugosa3 Malyavkhina, p. 28, pi. 13 fig. 5.

1970 Nevesisporites fossulatus Balme, p. , pi. 3 figs. 1-5

Description of specimens.

Microspores, trilete, essentially patinate. Amb circular.

Laesurae distinct, extend to the inner edge of the patina, often

slightly sinuous, accompanied by slightly raised lips. Equatorial and distal exine crassitudinous (2-4 microns thick) forming a patina which extends onto the equatorial region of the proximal surface, where it is delineated by the curvature of the contact faces. Patina deeply incised by distal, circumpolar ring of thinner exine. Width of incision varied from 0.5 - 6 microns.

Exine of contact faces thin, sometimes bearing very fine scat tered grana. - 132-

Dimens ions .

26 (31) 42 microns. 50 specimens measured.

Rema rk s.

Limatulasporites fossulatus (Balme) comb. nov. displays

an extremely broad morphological range. It is closely similar

to Limatulasporites sp. and possibly forms a continuous morpho

logical series with Retusotriletes radiatus (Kara Murza) comb,

nov. These forms could well be microspore variants of a single

parent plant. The polar crassitude within the circumpolar

incision is often slightly thicker at the edge and dependant

on the relative state of preservation displays a darker ring in

this vicinity. This tendency culminates in the occurrence of

a distinct L. fossulatus variant displaying an organisation

similar to Polyoingulatisporites Simoncsios & Kedves emend.

Playford & Dettmann 1965 .

Previous records.

This form has previously been reported from the uppermost

Scythian of the Olenek Stage in the northern Urals (Tschalyschev

& Varyukhina 1962) and the uppermost Permian Chhidru Formation

of the Salt Range (Balme 1970). A similar form (Selaginella

rarirugosa) is reported from the Late Triassic of Western Siberia

by Malyavkhina (1964).

Compa r i s on s.

Limatulasporites fossulatus (Balme) comb. nov. is extremely

similar to Limatulasporites sp. and is tentatively delineated by

its more constant circular amb , thicker and more prominent patina and larger size. However, these may not be particularly diagnostic characters. These forms occur commonly together - 133- throughout the lower and middle portions of the Narrabeen Group.

Size distribution curves suggest that they may possibly be distinguished on the basis of size, despite the small difference in mean size (23-32) and the overlap of size ranges. Retuso- triletes radiatus (?Kara Murza) comb. nov. is differentiated only by the absence of the circumpolar incision. Variants displaying "polycingulate" organisation are distinguished from

Polyoingulatisporites dejerseyi sp. nov. by the absence of the thick characteristic labrae of that species. L. limatulus

(Playford) comb. nov. has constant, more prominent proximal sculpture and has a cingulate rather than patinate exine organisat ion.

Occurrence.

Limatulasporites fossulatus first appears immediately above the ValesPoint Coal Member in Newvale D.D.H. No. 28. It occurs commonly throughout the lower and middle Narrabeen Group in middle sediments. It is extremely rare above the horizon of the

Bald Hill Claystone.

Limatulasporites limatulus (Playford) comb. nov.

PI. 15 figs. 10 - 18

Selected synonymy.

1965 Nevesisporites limatulus Playford, p. 188, pi. 8, figs.16-19.

? 1965 "unidentified spore" Tschalyschev & Varyukhina (in

Tschalyschev, Varyukhina & Molin) pi. 8, fig. 106.

1967 Retusotriletes olipeata Helby, p. 62, pi. 1 fig. 3

1967 Retusotriletes junior de Jersey & Hamilton, p. 3, pi. 1

f ig . 4 - 7 . - 134-

Description of specimens.

See Playford 1965, p. 188.

Dimens ions.

Equatorial diameter 28 (42) 50 microns. 25 specimens

measured.

Remarks.

Limatulasporites limatulus is a fairly common component of eastern New South Wales Mid to Late Triassic microfloras.

I have observed that as the relative state of preservation of the microflora falls off, the number of specimens possibly attributable to Retusotriletes elipeata Helby and R . junior de Jersey & Hamilton increases. I consider that these latter forms are preservation variants of L. limatulus. This is borne out by the similarity of organisation of the forms and the Coincidence of their respective size ranges. The presence of a distal crassitude is somewhat intermittent, but forms dis playing this feature are overwhelmingly predominant in most populat ions.

Previous records.

Limatulasporites limatulus has been reported from the Tiers

Formation of north-eastern Tasmania (Playford, 1965) , the Moola- yember Formation, Clematis Sandstone and upper part of the Rewan

Formation in south-eastern Queensland (de Jersey & Hamilton, 1967; de Jersey 1968).

Occurrence.

Limatulasporites limatulus first appears in the Tuggerah

Formation in Ourimbah Creek D.D.H. No. 5 and in the lower part - 135- of the Gosford Sub Group in the Balmain Shaft. It is a constant component of microfloras throughout the Hawkesbury Sandstone and the Wianamatta Group and their equivalents.

Limatulasporites sp.

PI. 15 figs. 10-12

Description of specimens.

Microspores, trilete, essentially patinate. Amb distinctly rounded triangular, occasionally sub-circular. Laesurae distinct, extend to inner edge of patina, often accompanied by slightly raised lips. Equatorial and distal exine crassitudinous (2 microns thick) forming a patina which extends slightly onto the proximal surfaces. Patina usually incised by a distal, circumpolar ring of thinner exine, up to 3 microns in width.

Incision often absent.

Dimens ions.

15 (23) 29 microns. 50 specimens measured.

Remarks.

As stated above, Limatulasporites sp. closely resembles

L. fossulatus and is only tentatively delineated from it. The constant mutual occurrence of these forms suggest that they may possibly be variants of a single parent species.

Compar is ons.

Limtulasporites sp. is tentatively delineated from

L. fossulatus (Balme) comb. nov. by its smaller size and tri angular amb. It lacks the narrow crenulated cingulum and broad labrae of Limatulasporites brunkeri sp. nov. If differs from forms assigned to Stereisporites antiquasporites (Wilson & - 136-

Web s t er) Dettmann by its longer laesurae and patinate organisation.

Occurrence.

Limatulasporites sp. appears immediately above the Vales

Point Coal Member in Newvale D.D.H. No. 28. It is a common component of lower and middle Narrabeen Group microfloras, becoming intermittently abundant above the top of the Munmorah

Conglomerate. It occurs as a rare component of Hawkesbury

Sandstone microfloras.

Genus POLYCINGULATISPORITES Simoncsics & Kedves emend. Playford

& Dettmann 1965.

Selected Synonymy.

1956 Chomotriletes Naumova (partim.), Bolkhovitina, p. 35.

1957 Sphagnites Cookson (partim.), Balme, p. 16.

1959 Annulispora {partim.) de Jersey, p. 358

1961 Polyoingulatisporites Simoncsics & Kedves, p. 34.

1962 Neoohomotriletes Reinhardt, p. 707.

1965 Poly oingulatisporites Simoncsics & Kedves emend. Playford

& Dettmann, p. 143.

Type species. Polyoingulatisporites oiroulus Simoncsics & Kedves

- original designation.

Remarks.

Playford & Dettmann (1965) emended and re-interpreted the genus Poly oingulatisporites Simoncsics & Kedves 1961 to include trilete, cingulate microspores with a distal, circumpolar, thickened exine ridge surrounding a polar crassitude. They indicate that Poly oingulatisporites is delineated from the similarly organised Tauroousporites Stover emend. Playford & - 137-

Dettmann 1965 by the absence of sculptural elements such as

grana, etc. They also suggest that Annulispora de Jersey 1959

(as well as the synonymous Distalanullsporltes Klaus 1960)

lacks a cingulum and a polar crassitude. Poly eingulatlsporites

differ from Limatulasporites gen. nov. in possessing two, distal

circumpolar zones of thinner exine.

Polycingulatisporites deg erseyi sp. nov.

PI. 16 figs. 1-9

Description of specimen.

Microspores, trilete, cingulate. Amb circular to rounded triangular, distal hemisphere often inflated but characteristically flat at the distal pole. Proximal surface often occurs as a low pyramid. Laesurae very prominent, usually straight although sometimes slightly sinuous in the immediate vicinity of the apex. They extend 3/4 radius, accompanied by thick lips. Lips comprised of low (1-2 microns) relatively flat although often gently undulating, exinal ridges (average width 3-5 microns).

These ridges are continuous, joining in the vicinity of the apex and beyond the lateral extremity of the laesura, where they rapidly narrow, and are often raised as an auricular nodule

(= terminal boss PI. 16 fig. 4). Equatorial and distal exine comprises a more or less continuous crassitude (2-4 microns thick) which is interrupted by two annular rings of markedly thinner exine. The rings have slightly irregular outline.

The outer surface of the crassitude is gently undulating.

Proximal surface is smooth. - 138-

Dimens ions .

Diameter 31 (38) 47 microns. 20 specimens measured from

s amp1e 5 4 7 .

27 (32) 37 microns. 20 specimens measured from

s amp1e 5 5 7 .

Overall size limit 27 - 54 microns.

Holo typ e.

Slide 556/3 33.7 105.8 PI. 16 figs. 1, 2. Size 43 microns.

Comparisons.

PoZycinguZatispovites dejevseyi sp. nov. is very similar to

P. cvenuZatus Playford & Dettmann, but has a predominantly cir

cular amb, a smaller size range (although there is a marginal

overlap) and more uniform labrae. I have not encountered

P. cvenuZatus in Triassic sediments in New South Wales to date.

LimatuZaspovites bvunkevi sp. nov. is closely similar, but differs

in having a single, distal, circumpolar incision , a smaller

size range (there is some overlap) and possessing a narrow, wavy

cingulum. PoZycinguZatispovites oZavus (Balme) comb. nov. *

has distinct, well spaced distal exine ridge and polar crassi

tude, rather than annular incision in the distal crassitude (or

patina).

* Footnote.

Playford & Dettmann (1965, p. 145) reassigned AnnuZispova

densata de Jersey to PoZycinguZatispovites. P. densatus (de

Jersey) Playford & Dettmann appears to be a junior synonym of

PoZycinguZatispovites cZavus (Balme) comb. nov. (Sphagnites

cZavus Balme 1957, p. 16, pi. 1 figs. 4-6). - 139-

Re ma r ks .

The inconsistent nature of circumpolar incisions in these

patinate species has been discussed above. The occurrence of

a single distal circumpolar incision in the patina of L. brunkeri

sp. nov. is the most diagnostic feature delineating it from

P. dejerseyi sp. nov. It is possible that these forms are

microspore variants of a single parent plant. However, because

of the apparent consistency of the delineating characters, these

forms are tentatively regarded as different species.

Occurrence.

Polycingulatisporites dejerseyi sp. nov. first appears in

the upper portion of the Munmorah Conglomerate in Ourimbah Creek

D.D.H. No. 4 and is a consistant but relatively rare component

of microflora extending to the top of the Patonga Claystone. It

has not been encountered above the top of the Bald Hill Claystone

or its equivalents.

Genus ANNULISPORA de Jersey 1960.

Type species. Annulispora follioulosa (Rogalska) de Jersey -

- original designation.

Annulispora sp. cf. A. follioulosa (Rogalska) de Jersey.

PI. 15 figs. 13, 14.

1954 Sporites follioulosa Rogalska, pp. 26, 44, pi. 12 fig. 8.

1960 Annulispora follioulosa (Rogalska) de Jersey, p. 7, pi. 2

fig. 2.

R e m a r k s .

Although only two specimens are recorded, both from the

Bringelly Shale, these occurrences significantly extend the - 140-

recorded range of the Annutispora group. There is some indi

cation that these specimens are slightly cingulate.

Suprasubturma LAMINATITRILETES Smith & Butterworth 1967

Genus CADARGASPORITES de Jersey & Paten 1964 emend.

Type species. Cadargasporites baoulatus de Jersey & Paten emend.

Reiser & Williams - original designation.

Emended diagnosis.

Microspores, trilete, Amb more or less circular. Contact

area prominent, bordered by a characteristic murus, comprised

of a double thickness of detached exoexine. Exine distinctly

two layed, although not necessarily totally cavate. Exoexine

on distal and equatorial surfaces may exhibit sculptural ele ments. Exoexine markedly thinner on the contact area, although

it may thicken in the immediate vicinity of the laesurae, not necessarily laevigate.

Remarks.

The original diagnosis of Cadargasporites by de Jersey &

Paten 1964, p. 5 indicates a two layered exine with the outer, ornamented layer (? exoexine) absent from the well defined contact area. Reiser and Williams (1969) presented an emended diagnosis which recognised the extension of the exoexinal layer onto the contact area. I consider the contact area exoexine murus to be the most diagnostic feature of the genus Cadarga sporites. This structure is comprised of a double layer of the exoexine. The murus often displays characteristic bosses at the termini of the laesurae.

Cadargasporites senectus de Jersey & Hamilton

PI. 17 figs. 7-9, pi. 18 figs. 22, 23 - 141-

Description of specimens.

Microspores, trilete with very prominent contact area.

Outline circular in polar view, oval to circular with a flat

tened contact area in lateral view. Laesurae distinct, often sinuous, extend to edge of contact area accompanied by trans parent, membranous lips (2-3 microns wide, 2-4 microns high) which pass into the murus surrounding the contact area. Contact area extremely prominent, surrounded by membranous exoexinal murus (PI. 17 fig. 8) 2-4 microns high, 1-1,5 microns wide at the base, slightly wider than half spore diameter. Murus thickens and is markedly higher at the junction with the laesurae lips, giving an auriculate appearance to some speci mens. Exine is layered although not obviously cavate apart from double layer of detached exoexine which comprises the proximal murus, 1.5 - 2 microns thick. Sculpture confined to distal surface and proximal surface outside contact area. It consists of fine, irregular microreticulation (lumens 1-1.5 microns wide, muri 0.5 - 1 micron wide), closely packed grana rugulae (up to 1 micron high). The sculpture becomes finer approaching the contact area. Contact area smooth.

Dimens ions.

Equatorial diameter 34 (56) 74. 50 specimens measured from sample 429.

Remarks.

Cadavgasporites senectus was proposed by de Jersey &

Hamilton (1967 pp. 8 - 9) to include forms possessing fine grana, coni and microrugulae. However, Wianamatta Group popu- - 142-

la t i o n s also include a microreticulate sculpture which is

actually predominant. Cadargasporites seneotus can be dis

tinguished from the Jurassic species described by de Jersey

and Paten (1964) only by the nature of the sculpture. C.

retioulatus de Jersey & Paten and C. baouZatus de Jersey & Paten

1964 display raised lips and murus thickenings similar to

C. seneotus.

Previous records.

Cadargasporites seneotus has been previously reported from

the lower and middle Moolayember Formation of Queensland, (de

Jersey & Hamilton 1967) A similar form from the Lashly Form

ation, Antarctica has been tentatively assigned to this species by Helby & McElroy (1969).

Occur rence.

Cadargasporites seneotus first appears in considerable abundance in the central portion of the Bringelly Shale. It extends throughout the younger Wianamatta Group section as a relatively constant component of the microflora. Occasional fragmentary specimens tentatively referred to this species are encountered in the upper part of the Hawkesbury Sandstone.

Cadargasporites wattsae sp. nov.

PI. 17 figs. 1-6, 10-14.

Description of specimens.

Microspores, trilete with very prominent contact area.

Outline circular in polar view, more or less circular with flat or slightly arched contact area in lateral view. Laesurae distinct, usually straight, extend to the edge of the contact 143- area accompanied by broad (up to 4 microns wide), low (about

1 micron) lips which thin markedly approaching the terminal boss. Contact area very prominent, delineated by a circumpolar exoexinal murus, comprised of a double layer of exoexine. Murus

2 - 3 microns high with distinct apical bosses at the termini of the laesurae. Exine distinctly two layered, often cavate.

Distal and equatorial exine 1 - 1.5 microns thick, surface covered with fine (about 0.5 microns diameter), closely packed grana. Exoexine on contact area thin with tendency to break up

(forming a hilate area) in interradial regions giving the impressions of grana or small verrucae on the proximal surface.

Intexine attached to exoexine at least under the surface of the contact face to the inner edge of the murus. Intexine smooth,

1-1.5 microns thick.

Dimens ions.

Exoexine - equatorial diameter 43 (59) 77 microns.

Intexine - " M 40 (53) 67 microns.

20 specimens measured from sample 726.

Exoexine - polar diameter 60, 53, 50, 44 microns.

Intexine - " " 57, 49, 47, 42 microns.

Type locality .

Balmain Shaft, dark grey shale at 1134 ft.

Holotype.

Slide 726/1 25.0 106.5 Illustration - PI. 17 fig. 4

(Equatorial diameter -

5 3 microns) - 144-

Comparisons .

Cadargasporites granulatus de Jersey & Paten emend.

Reiser & Williams possesses a wider range of distal and equa

torial sculptural elements, which appear to be intimately

related to an overall reticulate pattern. Cadargasporites

reticulatus de Jersey & Paten emend. Reiser & Williams is

distinguished by the projecting elements superimposed on a

scabrate or finely granulate exoexine. Cadargasporites

senectus de Jersey & Hamilton is distinguished by the distal

exoexinal sculpture and large membranous lips accompanying the

laesurae. Psomospora detecta Playford & Helby is superficially

similar but lacks a distinct circumpolar proximal murus, and

is not known to develop a cavate exinal organisation.

Occurrence.

Cadargasporites wattsae sp. nov. first appears in the uppermost portion of the Patonga Claystone. It has also been encountered in the upper portion of the Bulgo Sandstone, extending into the Bald Hill Claystone.

Cadargasporites sp. 1

PI.41 fig. 26.

Description of specimens.

Microspores, trilete with very prominent contact area.

Outline more or less circular in polar view, oval to circular with flattened contact area in lateral view. Laesurae distinct, often slightly sinuous, extending to edge of contact face accompanied by membranous labrae (1-2 microns wide, 2-3 microns high) which pass into prominent bosses on the contact murus. - 145-

Contact area prominent, surrounded by exoexinal murus, consist

ing of double layer of exoexine. Diameter of contact area

varies from 2/3 to almost full diameter of spores. Murus 2-4

microns wide, up to 5 microns high, thickening to forms pro

minent boss at the terminae of the laesurae. Exine layered,

cavate. Exoexine 2-3 microns thick, covered with fine (0.5-

1.5 micron basal diameter 0.5-1 micron high), closely packed

(0.5-1 micron apart) grana. Sculptural elements persist onto

contact face but are much smaller. Intexine smooth.

D i mens ions.

Equatorial diameter 60 (79) 101 microns. 21 specimens

measured.

Remarks.

The majority of specimens assigned to this species are

strongly carbonised compared to other elements of the micro

flora. Contact murus variously developed, often scarcely de

tectable in interradial area.

Comparisons.

C adargasporite s granulatus de Jersey & Paten emend. Reiser

& Williams has a scarcely discernable contact murus, and an

exoexinal sculpture which consists of grana and coni surmount

ing a fine reticulate ridge system. The size range of this

species as reported by Reiser & Williams (1969) is 37-58 microns. Cadargasporites senectus de Jersey & Hamilton has a

very prominent membranous contact murus, normally exhibits well

developed membranous labrae and usually displays a diversity

of exoexinal sculptural elements which do not pass onto the - 146- contact area. Cadargasporites wattsae sp. nov. has a thinner translucent exoexine, smaller contact area, often displaying patches of exoexine breakdown on the contact area.

Occurrence.

Cadargasporites sp. has only been identified from samples taken from the central portion of the Hawkesbury Sandstone.

Genus LYCOSPORA Schopf, Wilson & Bentall emend.Potonie & Kremp

1954 .

Type species. Lycospora micropapillatus (Wilson & Coe) Schopf,

Wilson & Bentall - original designation.

Remarks.

Smith & Butterworth (1967, p. 245) have pointed out the overall similarity of the organisational pattern of Lycospora to genera assigned to the Laminatitv'i'ietes. Lycospora goulburnensis sp. nov.

PI. 18 figs. 1-8

Description of specimens.

Microspores, radial, trilete, angulate. Amb rounded triangular to sub-circular, usually with finely dentate peri phery. Laesurae extend in excess of 3/4 radius, often indis tinct, but occasionally with narrow, slightly raised lips.

Specimens often exhibit "curvaturae perfectae". Exine not noticeably layered, 1-1.5 microns thick on distal surface, thinning towards pole on proximal surface. Distal and equa torial area covered by closely packed sculptural elements com prising grana and small verrucae. Grana 0.5 - 1.5 microns basal diameter, verrucae 1.5 - 2.5 microns basal diameter, - 147-

1.5 microns high. Verrucae usually confined to the centre of

the distal surface. Proximal surface laevigate although some

specimens are punctate. Cingulum varies in width from 2 - 6 microns, usually covered by sculptural projections.

Dimens ions.

Equatorial diameter 28 (35) 42 microns. 25 specimens

measured.

Hoio t ype.

Slide 327/4 18.0 113.0 Illustrations PI. 18 figs. 1-3.

Type locality.

East side of Cox's Gap Tunnel, 2 ft. above top coal seam.

Comp arisons.

Lycospora goulburnensis sp. nov. has a mean diameter in excess of the recorded maximum diameter of L. suratensis de

Jersey from probable Mid Carboniferous sediments below the

Surat Basin of Southern Queensland. Its sculptural elements are also coarser, distinct verrucae encountered as the dominent projection on some specimens. It has coarser sculptural elements and is considerably smaller than cf. Lycospora sp.

(Balme 1960, p. 28, pi. 5 fig. 1) from the Anderson Formation of the Fitzroy Basin, Western Australia. It is indistinguish able from microspores separated from Selaginella harrisiana

(Townrow, 1968).

Occurrence.

Lycospora goulburnensis sp. nov. is a relatively rare component of basal Narrabeen Group microfloras along the Goul- burn River, New South Wales. Single specimens were encountered - 148-

from the Bui go Sandstone in Wollongong D.D.H. No . 28 and below

the Vales Point Coal Member in Newvale D.D.H. No . 28 .

Genus UVAESPORITES Doring 1965 emend.

Type species. Uvaesporites glomeratus Doring - original

des ignation.

Selected Synonymy.

1964 Disoisporites Leschik emend, (partim.) de Jersey, p. 12.

1965 Uvaesporites Doring, p. 39

1969 Cadargasporites de Jersey & Paten emend, (partim.)

Reiser & Williams, p. 5.

Emended diagnosis.

Microspores, trilete with thickened equatorial exoexine

which may be interpreted or a cingulum. Exine layered, often

cavate. Distal and equatorial surfaces bearing massive sculp

tural elements which vary considerably although gemmae usually

predominate. Contact faces sharply delineated, smooth or with

very much reduced sculptural elements.

Rema rks.

Although Doring insists that the genus is acingulate he

describes and illustrates cingulate development. The layered

nature of the exine is apparent in illustrations of the holo-

type of the type species Uvaesporites glomeratus (Doring 1965, pi. 9 fig. 2) and in this instance could be interpreted as

cavate. The holotype of U. pseudoeingulatus (Doring, pi. 11

figs. 5-7) is clearly cavate exhibiting a detached, folded in-

texine. The concept of the genus is emended to include these characters. The diagnostic features of the genus are consi- 149 -

dered to be the predominance of massive sculptural elements,

particularly gemmae and the sharp delineation of the contact

faces. Cingulate development and cavate exine organisation do

not appear to be diagnostic at this level.

Gemmatriletes Pierce 1961 (Pierce 1961, p. 27) is morpho

logically similar. However, Pierce did not present a descrip

tive and comparative diagnosis for this genus and the single

illustration is inadequate for detailed comparison. Z-injispora

Hart 1965 is superficially similar but is characterised by

considerable merging of the bases of sculptural elements in

equatorial regions. Verrucosisporites bullatus Balme & Hennelly was re-assigned to Zinjispora by Hart (1965, b). I suggest

that this particular species is best recombined as Uvae sporites bullatus (Balme & Hennelly) comb, nov,

Uvaesporites verrucosus (de Jersey) comb. nov.

PI. 18 fig. 14 - 21

1964 Discisporites verrucosus de Jersey, p. 12, pi. 2

figs.13, 15, 16.

1969 Cadargasporites verrucosus Reiser & Williams, p. 6,

pi. 2 figs. 10-13, pi. 3 figs. 1, 2.

Description of specimens.

Microspores, trilete, incipiently cingulate. Amb circular to sub-triangular with convex sides and rounded corners, periphery interrupted by sculptural elements. Distal hemi sphere slightly less than hemispherical, proximal surface distinctly pyramidal in lateral view, Laesurae usually dis tinct simple or accompanied by narrow (0.5 - 1.5 microns wide) slightly raised labrae, extend in excess of 3/4 radius to edge - 150-

of contact face where they occasionally terminate against a boss projecting from the inner edge of the thickened equa

torial exoexine (=cingulum). Exine two layered, occasionally

cavate. Exoexine thickness variable, although cingulum up to

4 microns across is often developed. Equatorial and distal surface of exoexine bearing variety of sculptural elements including genumae (3-5 microns high, 2-3 microns basal diameter,

2-3 microns high outline variable), pilae (up to 4 microns high, basal diameter 1.5 microns, caput diameter 2-3 microns), coni

(up to 3 microns high, basal diameter up to 3 microns) and baculae (1.5 microns basal diameter, 2-3 microns high. Elements are usually discrete. Spacing of sculptural elements varies considerably from specimen to specimen. Contact area sharply defined, smooth or scabrate with thin, usually attached exine layers. Intexine smooth, relatively thin, occasionally folded.

Dimens ions.

Equatorial diameter exclusive or sculptural elements

23 (35.5) 44 microns. 20 specimens measured.

Rema rks.

De Jersey (1964, pp. 12, 13) interprets Uvaespovites verruoosus (de Jersey) comb. nov. as having a ring tenuitas or rimular and a non functional trilete apparatus. On this basis he tentatively assigns this form to the Coniferaphyta.

Although it may not be recommended to refer fossil material of this age to extant suprageneric taxa, it is abundantly evident that de Jersey regards this species as a pollen grain.

I believe that the feature interpreted by de Jersey (1964, - 151- pl. 2 fig. 13) as a ring-tenuitas is merely the cavity between the detached exine layers.

Reiser & Williams assign identical forms to Cadargasporites de Jersey & Paten 1964 emend. Reiser & Williams on the basis of the marked distinction of the thin, smooth contact area and its two layered exine. However, it lacks the circumpolar contact murus which is diagnostic of Cadargasporites. It is interesting to note that the morphology of Discisporites verrucosus de

Jersey and Cadargasporites verrucosus Reiser & Williams was no t compared.

Previous records.

Uvaesporites verrucosus (de Jersey) comb. nov. extends throughout the Bundamba Group (de Jersey 1964). It is also reported from the Moolayember Formation (de Jersey & Hamilton,

1967) although it was not identified in material from the Clematis

Sandstone (de Jersey, 1968) and the Wandoan Formation, (de

Jersey & Hamilton, 1969) of southern Queensland. Helby {in

Esso Exploration Inc. 1965 - unpublished) records its occurrence in the Wandoan Formation of northern New South Wales. Reiser

& Williams indicate that it ranges from the Precipice Sandstone to the lower portion of the Hutton Sandstone in the Early - Mid

Jurassic sequence of the Surat Basin, southemQueens1and.

Occurrence.

Uvaesporites verrucosus is first recognised in microfloras from the Hawkesbury Sandstone. It extends throughout the

Wianamatta Group and equivalent strata as the constant but minor microfloral component. - 152-

Uvaesporites bullatus (Balme & Hennelly) comb. nov.

PI. 18 figs. 9-11

1956b, Vevvucosispovites bullatus Balme & Hennelly, p. 250.

pi. 4 figs. 4 5-4 7

1965b , Zinjispora bullata (Balme & Hennelly) Hart, p. 129, text

figs. 330.

Description of specimens.

Microspores, trilete. Amb sub-circular to sub-triangular with convex sides and rounded corners. Periphery irregular due to projecting sculptural elements. Distal surface hemispherical, proximal surface forming a low pyramid. Exine not noticeably layered bearing very closely packed gemmae (up to 4 microns high,

2 microns basal diameter - these form a continuous gradation with pilae), verrucae (rounded outline up to 4 microns high and

6 microns basal diameter) and with small coni and grana inter spersed between the larger elements. Contact area well marked, exine thins approaching the apex although often bearing much reduced sculptural elements towards the edge of the contact area. Laesurae usually distinct, extend to edge of contact face, simple or labrae (lips 1-1.5 microns wide, less than 1 micron high - mainly delineated by differential staining).

Holo ty p e .

Although Balme & Hennelly (1956 b, p. 250) indicated the type locality of "Vevrucosisporites" bullatus they did not designate a holotype. Hart (1965 b, p. 129) has selected the specimen illustrated by Balme & Hennelly on Plate 4, figure 46 as leototype. In all instances, both in the text and on distribution diagrams, Perotriletes should read Perotrilites. - 153 -

Remarks .

The predominantly "bulbous" sculptural elements (as

described by Balme & Hennelly) and the clearly marked contact

area of this species indicate the close morphological relation

ship to other species of Uvaesporites Doring 1965. However,

I have not observed cingulate or cavate exine development in

this species.

Comp ar isons .

Uvaesporites bullatus (Balme & Hennelly) comb. nov. most

closely resembles U. verrucosus (de Jersey) comb. nov. but has

more closely spaced, usually finer sculptural elements. U.

verrucosus also intermittently displays a cingulum and cavate

exine organisation.

Oc curr enc e.

Although Balme & Hennelly (1956 b ) indicate that this

species is a fairly common component of Newcastle Coal Measures

microfloras it was not encountered in samples between and

including the Wallarah Seam and the Vales Point Coal Member. It

is encountered as a very rare component of basal most (lower

100 ft.) Narrabeen Group microfloras.

Genus PEROTRILETES Erdtman ex Couper emend. Evans 1970

Selected Synonymy.

1947 Perotriletes Erdtman, p. 111.

1953 Perotriletes Couper, p. 31.

1955 Kraeuselisporites Leschik, p. 36.

1958 Styxisporites Cookson & Dettmann, p. 114.

1962 Eeliosporites Schütz, p. 311.

1962 Kraeuselisporites Leschik emend. Jansonius, p. 46. - 154-

1962 Gondisporites Bharadwaj, p. 84.

1964 Indotritadites Tiwari, p. 251.

1964 Anulatizonites Maedler, p. 176.

1970 Perotriletes Erdtman 1947 ex Couper emend. Evans, p.

Type species. Perotriletes granulatus Couper emend. Evans

- designated by Couper (1953, p. 31)

Remarks.

Evans (1969) has reinterpreted the genus Perotriletes as being zonate rather than perinate. This reinterpretation is based on that authors examination of the type material of

P. granulatus (Couper) and is supported by the photographs he presents. Thus Evans' emended concept of Perotriletes encompasses trilete, zonate (and as defined - acavate), distally and equatorially sculptured (sculpture usually echinate) microspores. In discussing this emended diagnosis Evans regards

Sty xisporites Cookson & Dettmann 1958 as a junior synonym, but attempts to preserve Kraeuselisporites Leschik emend. Jansonius

1962 as a distinct taxon. Jansonius (1962) and Balme (1963) have previously suggested that Styxisporites and Kraeuselisporites were distinguishable by the nature of the lips accompanying the laesurae and the relative density of the zonal exoexine. How ever, Dettmann (1963) rejects these characters as diagnostic generic criteria in this particular case. From examination of a wide range of Upper Permian and Mesozoic forms of this general organisation I am inclined to agree with her. I there fore regard Kraeuselisporites as a junior synonym of Perotriletes. - 155-

Prior to the reinterpretation of Perotriletes by Evans I

had examined the type material of Kraeuselisporites dentatus

Leschik. The holotype was not obviously cavate and I

did not encounter cavate organisation in other representatives

of the population. However, a number of authors have used a

slightly broader interpretation of this genus (Balme, 1963;

Reinhardt & Schimtz, 1965; Helby, 1966 and Playford & Helby,

1968) assigning to it species which were comprised of or in

cluded representatives with distinctly cavate organisation.

Playford & Helby (1968, p. 112) discuss the occurrence of

cavate and acavate exinal organisations in an individual

species concluding that it is possibly the result of initial preservation of the spore and or the result of chemical pro cesses to which the spore is subjected during maceration. I suggest that the presence or absence of cavate exinal organi- Erdtman ex Couper emend. Evans 1970, Lundbladispora sation in genera such as Perotriletes^ Balme 1963 and Aratrz- spor ites Leschik emend. Playford & Dettmann 1965 (these genera usually have lycopsid affinities) is not necessarily a defini tive generic character.

Lundbladispora Balme emend. Playford 1965 has an overall organisation closely similar Perotriletes. However, all species presently assigned to Lundbladispora are characterised by three interradial papillae on the proximal surface of the intexine. This would appear the only reliable feature with which these genera can be distinguished.

Perotriletes differens (Helby) comb. nov.

PI. 20 figs. 5 7 - 156-

Selected Synonymy.

1967 Kraeuselisporites differens Helby, p. 65, pi. 2 figs. 23-27 .

1967 Kraeuselisporites verruoifer de Jersey & Hamilton, p. 11,

pi. 6 figs. 1, 2, 5, 6.

D e s c r i p t i o n of specimens.

See Helby 1967, pp. 65, 66.

R e m a r k s .

Perotriletes differens (Helby)comb. nov. often exhibits a characteristic area of darkened exine at the base of the zona, which is associated with extremely close spacing of the sculptural elements. De Jersey (1968, p. 10) suggests that the darkening is evidence of an equatorial crassitude and that the spacing of the sculptural elements in this region is a primary feature. However, I interpret these features as resulting from compaction of a previously inflated distal hemis^phere on which sculptural elements are more or less evenly distributed. The even distribution of sculptural ele ments is exhibited by specimens compressed in planes containing the polar axis. If this interpretation is accepted it is clear

that Perotriletes differens (Helby) comb. nov. and "Kraeuseli sporites " verrueifer de Jersey & Hamilton are synonymous.

Occur r en c e .

Perotriletes differens first appears in the upper portion of the Narrabeen Group. It extends throughout the Hawkesbury

Sandstone and Wianamatta Group, attaining maximum prominence in the upper portion of the Hawkesbury Sandstone and in the

Liverpool Sub-Group of the Wianamatta Group. - 157-

Pevotriletes kuttungensis (Playford & Helby) comb. nov.

PI. 19 fig. 8, 9.

1968 Kraeuselispovites kuttungensis Playford & Helby, p. 112,

p i . 11 f igs . 6,7.

Description of specimens.

See Playford & Helby (1968, p. 112-113.)

Remarks.

Specimens assigned to Pevotviletes kuttungensis (Playford

& Helby) comb. nov. are indistinguishable from the population described by Playford & Helby (1968). The presence of this species and several other forms diagnostic of the Grandispora microflora suggests that these specimens are recycled from

Carboniferous source areas to the north of the sample location.

Occurrence.

Several specimens of Pevotviletes kuttungensis were re corded in samples 991 and 1006.

Pevotviletes cuspidus (Balme) comb. nov.

PI. 20 figs. 8-11

1963 Kraeuselispovites cuspidus Balme, p. 19, pi. 5 figs.9-11

Description of specimens.

See Balme 1963 pp. 19, 20.

Dimens ions.

Equatorial exoexine diameter 52 (63) 78 microns. 10 specimens

me as ur ed.

Re m a r k s .

The Sydney Basin Perotviletes cuspidus representatives have a slightly smaller mean size than the type population. They include both cavate and acavate forms, on which the zona is often - 158- much reduced or occasionally absent.

Previous records.

PerotviZetes cuspidus is reported from the Scythian

Kockatea and Blina Shales of Western Australia (Balme, 1963).

It is also recorded from the Triassic Ross Formation of Tas mania (Playford, 1965). Balme (1970)has noted its occurrence in the Late Permian Chhidtu Formation and the Scythian Mianwali

Formation of the Salt Range.

Occurrence.

PerotviZetes ouspidus (Balme) comb. nov. is first encountered just above the base of the Munmorah Conglomerate. The highest record of its occurrence is in the upper portion of the Patonga

Claystone. It is invariably a rare constituent of the micro floras .

? PerotriZetes paZZidus (de Jersey) comb. nov.

P1. £ 1 figs. 1-4-

1962 CinguZatispovites paZZidus de Jersey, p. 6, pi. 2 figs.4,5.

Description of specimens.

Microspores, radial, trilete, cingulate, often cavate. Amb sub-circular to triangular, sides usually convex or occasionally straight, corners well rounded. Distal surface more or less hemispherical, proximal surface distinctly pyramidal. Laesurae distinct, labrate (lips 0.5 - 1 microns wide 1-1.5 microns high) extending to the inner edge of the cingulum. Exine layered, often cavate, exoexinal cavity usually markedly triangular.

Exoexine 1 - 2.5 microns thick, differentiated into a cingulum at the equator. Cingulum 2 - 6 microns wide, usually slightly - 159- wider in the interradial regions, devoid of sculptural elements, usually membranous towards the outer edge, Exoexine of distal surface bears wide variety of sculptural elements including spines (1.5 - 3 microns high, 1 - 1.5 microns basal diameter) pilae (2-3 microns high, 1 - 1.5 microns basal diameter, up to 3 microns at the expanded tip) irregular coni, verrucae and rugulae the bases of which merge to form an imperfect reticulate pattern. Exoexine on proximal surface smooth or finely spongeous.

Intexine smooth, less than 1 micron thick, usually in contact with exoexine along the length of the laesurae.

Dimens ions .

Equatorial exoexinal diameter 26 (33) 41 microns.

Equatorial intexinal diameter 16 (24) 27 microns. 20 specimens

measured from sample 940.

Polar diameter 20 - 27 microns. 4 specimens measured from

s amp 1e 9 4 0.

Remarks.

Although it is not possible to compare these specimens directly with the illustrations of Cingulat'Lspor'ites pallidus presented by de Jersey (1962, pi. 2, figs. 4, 5) they conform closely to the description of that species, but displaying a slightly smaller mean size. The species is tentatively re combined with PerotriZetes Erdtman ex Couper emend. Evans 1970.

Reservation is expressed because of the prominent occurrence of a distal, confused, reticulum which has not been assigned previously to the genus. I interpret Limbosporites Nilsson

1958 as being distinguished by a foveolate or foveo-reticulate - 160-

distal surface.

Previous records.

Perotritetes pattidus (de Jersey) comb. nov. has been

previously reported only from coals of the Ipswich Coal Measures,

south eastern Queensland, (de Jersey, 1962).

Occurrence.

Perotritetes pattidus was first recognised in the central

portion of the Grose Sandstone. It is a relatively rare com

ponent of younger Narrabeen Group and Hawkesbury Sandstone

microfloras becoming more common in the Wianamatta Group. It

attains maximum prominence in microfloras extracted from Wiana matta Group coals.

Perotritetes raniganjensis (Bharadwaj) comb. nov.

PI. 19 figs. 1-7

1962 Gondisporites raniganjensis Bharadwaj, p. 85, pi. 4

figs. 66, 67.

1964 Indotriradites korbaensis Tiwari, p. 252, pi. 1 figs, 4a,

4b , 5 , 6.

Description of specimens.

Microspores, trilete, cavate and cingulate (=zonate).

Amb sub-circular to rounded triangular with convex sides and

rounded corners. Distal surface slightly less than hemispherical,

proximal surface forms a low pyramid. Laesurae usually distinct,

extending 3/4 radius to inner edge of cingulum, more or less

straight accompanied by thin membranous lips standing up to 6 microns above general surface. Exine distinctly layered, cavate,

although exine layers usually in contact along laesurae. Exo- - 161- exine 2 microns thick distally, thickening equatorially to form narrow cingulum which usually extends into thin trans lucent zona (up to 8 microns wide). Exoexine spongeous bearing coni (2.5 microns basal diameter, 2-3 microns high), and spines

(up to 7 microns long, 5 microns basal diameter which taper rapidly to a point 2-3 microns above base). Spines and coni scattered 1.5 - 5 microns apart, surface between sculptural elements appearing granulate. Exoexine thinner on proximal surface, smaller sculptural elements confined to equatorial extremities, surface spongeous. Intexine smooth, often folded, less than 1 micron thick.

D imens ions.

Equatorial diameter, exoexine 52 (84) 107 microns

intexine 39 (61) 73 microns.

25 specimens measured from sample 992.

Remarks.

In proposing the montypic genus Gondisporite s Bharadwaj

(1962, p. 84) stated that the exoexine was granulate with scat tered large baculae. The illustrations of the type species,

G. raniganjensis (Bharadwaj 1962, pi. 4 figs. 66, 67), although rather poor, suggest a spongeous exoexine with a microgranulate surface expression. The organisation of this form is closely a analogous to the interpretation of Kraeuselisporites Leschik emend. Jansonius as illustrated by Balme (1963, text fig. 2) and consequently G. raniganj ensis Bharadwaj is recombined with

Perotriletes Erdtman ex Couper emend. Evans 1970. Tiwari (1964, p. 251) proposed the monotypic genus Indotriradites, to encompass - 162- cavate, cingulate, trilete microspores with an "intramicro- punctate" exoexine which has a "minutely serrate" peripheral outline and bearing large, scattered spines. It is clear that the organisation of this form is indistinguishable from Balme’s

(1963 , text fig. 2) interpretation of KraeuseZisporites and can thus be regarded as a junior synonym of PerotriZetes.

The morphology of Gondisporites raniganj ensis Bharadwaj and Indotriradites korbaensis Tiwari is obviously closely similar. Tiwari has attempted to distinguish the forms on the basis of the unstructured exoexine of G. raniganjensis.

In view of my interpretation of the exoexine of that species

I cannot accept Tiwari's distinction. There are differences in the size ranges of the respective type populations. However, these differences are more than covered by the size range of the population assigned to PerotriZetes raniganjensis (Bharadwaj) comb. nov. There exists a complete gradation (in several samples) between specimens displaying distinct spines and those dis playing coni. In poorly preserved material the larger sculptural elements are reduced to small verrucae. Comp ar i sons.

PerotriZetes euspidus (Balme) comb. nov. has less densely packed sculptural elements (6-10 microns apart) with longer spines which usually display a spongeous texture. LundbZadi- spora wiZZmotti Balme has considerably smaller spines, and lacks a distinct cingulum - zona development. PerotriZetes differens

(Helby) comb. nov. has a greater range of more closely set - 163- sculptural elements. The exoexine of this species is not noticeably structured.

Previous records.

Bharadwaj (1962) records "Gondisporites" raniganjensis from the Raniganj Coal Measures of India (Mid-Late Permian).

Tiwari (1964) has identified Indotriradites korbaensis from the Barakar Stage (?Mid Permian) of India.

Occurrence.

Perotriletes raniganjensis (Bharadwaj) comb. nov. is first recognised in samples 991, 992, immediately below the Vales

Point Coal Member, where it occurs as a prominent component of the microflora. It is a rare but fairly constant component of basalmost Narrabeen Group microfloras.

Genus LUNDBLADISPORA Balme emend. Playford 1965.

Type species. Lundbladispora willmotti Balme 1963 - original

des ignat io n .

Remarks.

Balme (1963, p. 21) defined Lundbladispora as a cavate, incipiently zonate microspore, with spongeous exoexine which could bear additional sculptural elements and an intexine characterised by three interradial papillae on the proximal surface. He assigned three species to Lundbladispora including

L. willmotti, L. brevioula and L. playfordi. The two former species were distinguished by projecting sculptural elements.

In emending Densoisporites Weyland & Krieger, Dettmann (1963, p. 83) outlined an essentially similar form genus to Lundbladi spora Balme 1963, but characterised by the absence of projecting - 164-

sculptural elements. She recombined L. playfordi Balme with

Densoisporites. Playford (1965) formally emended Lundbladispora

to exclude forms with a sculpture exoexine.

I consider the interradial papillae of the intexine of

Lundbladispora to be a significant diagnostic feature. These

appear to delineate Lundbladispora from Perotriletes[Erdtman ex Couper emend. Evans 1970 (=Kraeuselisporites)]species

occurring in the Sydney Basin sequence.

Lundbladispora brevioula Balme

PI. 20 figs. 1-4

1963 Lundbladispora brevioula Balme, p. 23, pi. 4, figs. 8,9.

Dimens ions.

38 (47) 64 microns. 10 specimens measured.

Remarks.

Specimens assigned to Lundbladispora brevioula are seldom well preserved. They exhibit a slightly larger size range

than that indicated by Balme (1963, p. 24).

Previous records.

Lundbladispora brevioula is reported the Kockatea Shale

and Blina Shale of Western Australia (Balme, 1963). It has been identified in a microflora from the Ross Formation of northern Tasmania (Playford, 1965). Balme (1970) reports its

occurrence in the Early Triassic Mianwali Formation and Mid

Triassic Tredian Formation of Pakistan.

Occurrence.

This form first appears in the Scarborough Sandstone and its

equivalents. It is relatively consistent in microfloras from - 165- the central portion of the Narrabeen Group, extending almost to the base of the Gosford Sub-Group. Isolated specimens have been encountered in microfloras from the Hawkesbury Sandstone.

Lundbladispora fibulata (Hennelly) comb. nov., emend.

PI. 21 figs. 5-17

1958 C'ivvatv'ivad'ites fibuZatus Hennelly, p. 366 , pi. 5 figs. 8,9.

? 1962 EeZiosporites altmarkensis Schultz, p. 311, pi. 1 fig. 9

pi. 2 figs. 10, 11.

1970 Kraeuselisporites raZZus Balme, p. , pi. 4 figs. 9-13.

Holotype.

Although Hennelly (1958) indicated the type locality of

" Civratvirad'tate s ” fibuZatus he did not assign as holotype.

The specimen illustrated by Hennelly (1958, pi. 5 fig. 9) is chosen here as a lectotype. This specimen has been rephoto graphed and is illustrated on pi. 21 fig. 8.

Description of specimens.

Microspores, trilete, often cavate and zonate. Amb circular to sub-triangular with convex sides and rounded apices. Laesurae distinct, often slightly sinuous, usually lipped (lips up to

3 microns wide, 3 microns high), extend to edge of intexine but are often projected to the edge of the zona by folding. Exine distinctly layered, usually cavate. Exoexine, 1-2 microns thick, spongeous but bearing fine attenuated spines, which often thicken and occasionally branch at the extremities. Spines extremely prone to breakage. Exoexine thins noticeably approaching apex.

Exoexine usually differentiated into thin, irregular, sculptured zona (up to 7 microns across). Intexine thin, bearing three - 166-

inter radial papillae.

Dimens ions.

Equatorial diameter of exoexine 29 (43) 57 microns.

Polar " " " 40 (40) 34

20 specimens measured from slide 985/4.

Remarks.

Although the specimens illustrated by Hennelly (1958)

are poorly preserved, it is possible to ascertain the scabrate -

spongeous nature of the detached exoexine. Also, a few speci mens in the type material exhibit a number of broken spines.

A complete gradation between specimens completely denuded of

spines to fully spinose - zonate forms is available in samples

985, 986 or 1006. A selection from this gradation is illustrated

on plate 21.

The forms assigned to Lundbladispora fibulata completely

encompass nKraeuselisporites" rallus Balme, although they have

a slightly smaller mean size. "Heliosporites" altmarkensis

is superfically similar, although the presence of the apical

papillae on the intexine should be established before this form

is accepted as a junior synonym.

Previous records.

Lundbladispora fibulata has previously been reported from

the basal Narrabeen Group in the Sydney Basin (Hennelly, 1958).

Balme 1970, records its occurrence in Late Permian Chhidru

Formation microfloras of Pakistan, as a rare to dominant form.

It has also been encountered in Late Permian - Triassic strata

from the Bonaparte Gulf Basin of Western Australia (Dr. E. Kemp, pers. oomm. )t - 167-

Occurrence.

Lundbladispora fibulata is a fairly constant and often prominent component of basalmost Narrabeen Group microfloras.

Above this it extends as a very rare microfloral component into the central portion of the Narrabeen Group.

Lundbladispora willmotti Balme PI. 23 figs. 10-12

1963 Lundbladispora willmotti Balme, p. 22, pi. 5 figs. 1-3 Description of specimen.

See Balme 1963, p. 22 Remarks.

The specimens assigned to Lundbladispora willmotti agree in all respects with the type population described by Balme (1963), although the local specimens invariably display lower exoexine:intexine diameter ratios.

Occurrence.

Lundbladispora willmotti is first encountered as a rare component of basal Narrabeen Group microfloras immediately above the Vales Point Coal Member. It occurs intermittently throughout the Clifton Sub-group. Genus DENSOISPORITES Weyland & Kreiger emend. Dettmann 1963. Type species. Densoisporites velatus Weyland & Krieger emend.

Dettmann - original designation.

1953 Densoisporites Weyland & Krieger, p. 12. 1961 Selaginella Spring (partim.) Krasnova (in Samoilovich et al.)

p . 19 .

1963 Lunbladispora (partim.), Balme, p. 21. - 168-

1964 Lygodiidites Pocock, p. 180.

? 1964 Cingulatizonites Maedler, p. 190.

Remarks.

Dettmann (1963, p. 85) emended Densoisporitesj interpreting

it as a cavate microspore, with a spongeous, unsculptured,

incipiently cingulate exoexine and a thin intexine bearing

three apical, interradial papillae. She also indicates that

forms described as Lundbladispora play fordi by Balme (1963)

should be recombined with Densoisporites. Pocock (1964, p.180) proposed the form genus Lygodiidites to encompass cavate micro

spores with a spongeous exoexine (see descriptions of L. laevigatus and L. balmei). The presence of apical papillae on the intexine was not mentioned by Pocock. However, these are evident on the holotype of Lygodiidites laevigatus (PI. 5 fig. 2). I regard Lygodiidites Pocock as a junior synonym of Densoisporites.

It is difficult to interpret the organisation of Cingulatizonites

Maedler although the illustrations (Maedler, 1964, pi. 2 figs.

18, 19) clearly indicate a cavate exine and suggest a dense, possibly spongeous exoexine. There is a slight suggestion of intexinal apical papillae on the holotype of Cingulatizonites rhaeticus (PI. 2 fig. 19), although these are not directly evident.

Densoisporites playfordi (Balme) Dettmann

PI. 22 figs. 12-14

Selected Synonymy.

1963 Lundbladispora playfordi Balme, p. 23, pi. 5 figs. 4-8.

1963 Densoisporites playfordi (Balme) Dettmann, p. 83. - 169-

Description of specimen.

Microspores, trilete, cavate. Amb. sub-circular to convex triangular. Distal surface hemispherical passing up proximally into saucer shaped cingulum in lateral view; proximal surface pyramidal. Laesurae distinct, extending to edge of intexine, although often projected across cingulum by folding. Laesurae accompanied by exoexinous lips up to 2 microns wide, 2-4 microns high. Exine distinctly layered, cavate, although exoexine and intexine usually in contact along the laesurae. Exoexine about

2 microns thick, apart from cingulum, spongeous, differentiated into distinct cingulum at equator. Width of cingulum variable, up to 7 microns. Exoexine thins noticeably on proximal face, occasionally folding back from the apex. Intexine thin, smooth apart from apical papillae which were seldom evident.

Dimens ions.

Equatorial diameter - exoexine 43 (52) 64 microns. 10 specimens measured from sample 555. Intexine 32 (42) 53 microns.

Maximum equatorial diameter of exoexine 87 microns (sample 75).

Remarks.

The morphology of population assigned here to Densoisporltes playfordi differs significantly from the type material illus trated by Balme (1963, pi. 5 figs 4-8). The Sydney Basin forms have a much lower exoexine:intexine diameter ratio and a more distinct cingulum, although the development of this latter structure is rather variable. The presence of intexinal apical papillae is only intermittently obvious. However, examination of a broad range of D. playfordi from the Kockatea Shale (slides - 170- kind ly provided by Dr. B.E. Balme) suggests that the local forms can still be accommodated by this species. Specimens assigned to D. playfordi from Late Permian and Early Triassic strata of Pakistan by Balme (1970) more closely resemble the

Sydney Basin population.

Balme (1963, p. 22) draws attention to the similarity of

D . playfordi to the microspores associated with Selaginellites polaris Lundblad from the Early Triassic of Greenland.

Previous records.

Densoisporites play fordi is reported from the Early Triassic

Kockatea Shale of the Perth and the Blina Shale and Erskine

Sandstone of the Fitzroy Basin (Balme, 1963). Playford (1965) reports its occurrence in a microflora from the Ross Formation

(?Early Triassic) of northern Tasmania. Balme (1969) suggests that this species characterises the Scythian microfloras of

Western Australia. He also indicates that the species ranges through the Late Permian Chhidru Formation and the Early Triassic

Mianwali Formation of the Salt Range, Pakistan.

Comparisons.

Ly godiidites balmei Pocock is similar to the Sydney Basin population of Densoisporites playfordi although it displays heavy plicate lips accompanying the laesurae which are not common in the local material. Densoisporites poatinaensis

Playford also has strongly developed lips which attain overall widths of 10 microns. The specimens illustrated by Playford

(1965, pi. 9, figs. 16, 17) would, however, fall within the morpological range of the Sydney Basin population of D. playfordi. - 171-

It is unfortunate that Playford did not make a direct com parison of these species. Densoispovites nejburgii (Schulz)

Balme has a circular amb and a smaller, restricted size range.

It also lacks a cingulum.

Occurrence.

Densoispovites playfordi first appears in the central portion of the Munmorah Conglomerate and extends almost to the base of the Newport Formation. It attains maximum prominence in the Patonga Formation to the north of Sydney.

Densoispovites navvabeenensis sp. nov.

PI. 22 figs. 15-19

Description of specimens.

Microspores, trilete, cingulate. Amb sub-triangular to triangular, sides rounded convex to straight (although distal surface below cingulum of sub-circular), corners sharply rounded. Distal surface helmet shaped in lateral view; proximal surface usually forms a low pyramid, often scarcely projecting above the level of the cingulum. Laesurae usually distinct, simple or accompanied by narrow exoexinous lips (1-1.5 microns wide) which are slightly raised and extend almost to the inner edge of the cingulum. Laesurae situated on slight arches of

the proximal surface, along which folds may develop. Exoexine

1-2 microns thick on distal surface, spongeous, although it may appear structureless and smooth in poorly preserved material.

Cingulum narrow, varying from 1.5-4 microns in width, often broadening adjacent to termini of laesurae giving an auriculate appearance. Intexine usually in contact with exoexine over - 172- proximal surface, smooth, occasionally displaying apical papillae, shape roughly paralleling amb. Markedly cavate speci mens exhibit typically triangular exoexine with a sub-circular intexine.

Dimensions.

Equatorial diameter 37 (43) 47 microns. 20 specimens measured

from sample 555.

37 (48) 60 microns. 20 specimens measured

from sample 642.

Type locality.

Ourimbah Creek D.D.H. No. 5 at 380 ft. (Patonga Claystone)

Holo type .

Slide 555/2 40.7 107.0 Illustration PI. 22 fig. 18.

Comparisons.

Balme (1970) indicates that Densoisporites ne jburgii

(Sculz) Balme is acingulate with a predominantly circular amb. densoisporites playfordi (Balme) Dettmann has a larger mean size, a broader cingulum and a considerably flatter distal surface. It also has a slightly thicker, more obviously spongeous exoexine.

Occurrence.

Densoisporites narrabeenensis sp. nov. first appears in the Scarborough Sandstone and its equivalents and extends to the base of the Bald Hill Claystone. It is often a dominent form in the central portion of the Narrabeen Group.

Genus DENSOSPORITES Berry emend. Butterworth et at. (in Staplin

& Jansonius, 1964) - 173-

Type species. Densosporites oovensis Berry - possibly designated

by Schopf, Wilson & Bentall (1944, p. 40)

Remarks.

Densosporites Berry has been emended variously by Schopf,

Wilson & Bentall (1944), Potonie & Kremp (1954), Bharadwaj &

Venkatachala (1962) and Butterworth, Jansonius, Smith & Staplin

(in Staplin & Jansonius, 1964). The latter proposed emendation has resulted from consultations of a committee of the Interna tional Commission for the Microflora of the Palaeozoic which has been studying representatives of the "densospore" group.

These proposals are tentatively accepted.

As interpreted by Butterworth et at. Densosporites encom passes trilete, cingulate, microspores with sub-triangular to circular ambs. The exine is distinctly layered with a thin, smooth intexine which may exhibit apical papillae. Exoexine of extremely variable thickness; smooth, scabrate or granulose on contact area; psilate, granulate, spinose - apiculate, verrucate on distal and equatorial surfaces. Proximal surface of cingulum usually projects above general surface of the contact area.

Although they specifically describe the layered nature of the exine of Densosporites these authors make no mention of a possible cavate organisation. The development of this type of exine organisation has been demonstrated in Densosporites sphaero- triangularis Kosanke by Hughes, Dettmann & Playford (1962).

It is also indicated by intexinal folding in D. anulatus (Loose)

Schopf et at. (Staplin & Jansonius, 1964, pi. 18 fig. 4, 29) and D. intermedius Butterworth & Williams (Staplin & Jansonius - 174-

1964 , pi. 18 figs. 6, 11). Dens ospordtes Berry emend. Butterworth et al. 1964 is distinguished from Densodspordtes Weyland & Krieger emend.

Dettmann 1963 by the variously thick, dense exoexine and cingulum which is usually without a spongeous structure. Densod- spordtes lacks distal or equatorial projecting sculpture. The contact face of Dens odspordtes usually forms a low pyramid which projects above the cingulum. Lundbladdspora Balme emend.

Playford 1963 is normally distinguished by its thinner spongeous exoexine. I suspect that forms described by Balme (1970) as

Lundbladdspora obsoleta might best be recombined with Denso- spordtesj despite its distinct spongeous exoexine. Anulatd- zondtes Maedler 1964 would appear to be a junior synonym of

Densospordtes Berry emend. Butterworth et al. 1964.

Densospordtes eonollyd sp. nov.

PI. 23 figs. 1-9

Description of specimens.

Microspores, trilete, cingulate. Amb circular to rounded triangular, periphery smooth or interrupted by sculptural ele ments, dependant on development of "zona". Distal furface less than hemispherical, contact area almost flat to slightly arched, seldom projecting above the proximal surface of the surrounding cingulum in lateral view. Laesurae usually distinct, extremely variable. They may be simple or labrate extending 1/2 to 2/3 radius, almost to inner edge of the cingulum, often terminating against a raised boss projecting from the inner edge of the cingulum. Exine layered often distinctly cavate. Thickness of 175- exoexine extremely variable; arranged as a cingulum on equatorial surface but appears to thin towards the distal pole.

Cingulum often "bizonate" (Staplin & Jansonius, 1964, text fig. 1), total width 6-15 microns, thin equatorial zona up to

5 microns across but not always evident. Exoexine sculpture extremely variable, ranging from almost smooth, scabrate to granulate, apiculate (spines 2.5 microns basal diameter, 1.5 -

2 microns high, often mammoid - see Staplin & Jansonius, 1964) to verrucate (up to 3 microns basal diameter, 1.5 - 2 microns high, irregular outline, closely spaced) on distal and equatorial surfaces. Exoexine sharply delineated at inner edge of cingulum, thinning significantly at edge of the contact area, smooth, punctate, scabrate or finely granulate. Intexine 1 micron thick, smooth, often folded, apical papillae were not identified.

Dimens ions.

Equatorial diameter 48 (62) 80 microns. 20 specimens measured

from s amp 1e 9 4.

intexine 22 — 56 "

Equatorial diameter 49 (60) 71 microns. 10 specimens measured

from sample 7 74.

Type locality.

Camden G.R. 691.836 (Annan Shale)

Holotype .

Slide 94/1 30.5 114.4 Illustrations PI. 23 figs. 7, 8.

Remarks.

The concept of Densosporites eonnollyi sp . nov. outlined above obviously encompasses an extremely broad range of morpho- - 176-

log i c a 1 variation. The intermittent occurrence of the equatorial

zona and the broad range of sculptural elements on specimens

occurring in a single sample lead me to suspect that this vari

ation is at least partly due to secondary mechanisms. However,

the considerable number of well preserved specimens indicate

that the greater part of the sculptural variation is a primary

feature.

Comp ar isons.

Anulati zonite s rotundus Maedler appears to be accommodated within the range of D. conoityi sp. nov. However, the illustra

tion presented by Maedler (1964, pi. 2 fig. 3) precludes a

detailed comparison of the species.

Occurrence.

Densosporites conollyi sp . nov. is first identified from

the Newport Formation of the Narrabeen Group. It extends

throughout the Hawkesbury Sandstone, the Wianamatta Group and

their equivalents as a fairly common microfloral component.

Genus CIRRATRIRADITES Wilson & Coe 1940.

Type species. Cirratriradites saturni (Ibrahim) Schopf, Wilson

& Bent al1.

Cirratriradites maeulatus Wilson & Coe was designated as

type species by Schopf, Wilson & Bentall (1944, p. 43). However,

Potonie & Kremp (1954, p. 162) indicate that this species is a junior synonym of C. saturni (Ibrahim) Schopf, Wilson & Bentall.

Remarks.

The meagre generic diagnosis of Cirratriradites given by

Wilson & Coe was expanded considerably by Schopf, Wilson & - 177-

Ben t a 11 (1944). These authors interpreted Cirratriradites as a trilete, cingulate microspore, with distal and equatorial sculpture which may consist of discontinuous radial ridges or form a distinct reticulate pattern, resulting in a serrate periphery. Laesurae are labrate and usually prominent. Smith

& Butterworth (1967) present a slightly more comprehensive interpretation in which they include a foveolate sculpture on the distal surface. The cavate nature of the exine of Cirra triradites elegans (Waltz) Potonié & Kremp was demonstrated by Hughes, Dettmann & Playford (1962). Smith & Butterworth suggest that this organisation could be regarded as common for the genus as a whole.

The distinctions between Cirratriradites Wilson & Coe 1940,

Densosporites Berry emend. Butterworth et al. and Cingulizonates

Dybova & Jachowicz emend. Butterworth et al. are not at all clear. These latter genera are apparently cavate, may exhibit apical papillae on the intexine and are characterised by a vacuolate exoexine (see Staplin & Jansonius, 1964). These features possibly also apply to Cirratriradites. The three genera are tentatively distinguished by the nature of the distal sculptural organisation. Densosporites and Cingulizonates are characterised by discrete, grana, coni, spines or verrucae.

Cirratriradites bulgoensis sp. nov.

PI. 22 figs. 1-11

Description of specimens.

Microspores, trilete, cingulate, cavate. Amb sub-triangu lar, sides convex with rounded corners, periphery serrate due - 178- to nature of exoexine sculpture. Distal surface hemispherical, proximal surface forms a low pyramid in lateral view. Laesurae distinct, usually labrate (lips 1 - 1.5 microns wide, up to 3 microns high), extend almost to inner edge of cingulum, often slightly sinuous. Exine distinctly layered, cavate. Exoexine and intexine in contact along the length of laesurae. Exoexine up to 3.5 microns thick on distal surface, inclusive of sculpture

Exoexine vacuolate rather than spongeous. Distal and equatorial surface finely foveolate (about 1 micron across) to distinctly foveo-reticulate (lumens polygonal up to 3 microns diameter, muri

2 microns high, 1.5 - 2.5 microns wide often displaying small foveolae = vacuoles). Exoexine thickened into distinct cingulum

(3-7 microns wide) at equator. Cingulum usually maintains width around entire periphery, thins slightly away from spore cavity.

Proximal exoexine noticeably thinner, usually smooth although poorly preserved specimens appear punctate. Intexine smooth, thin, apical papillae not observed.

Dimens ions.

Equatorial diameter - exoexine 35 (43) 54 microns.

20 specimens measured from sample 453

intexine 25 (33.5) 41 microns.

Type locality.

Camden D.D.H. No. 61 at 1183 ft. (lower portion of Bulgo

Sands tone) .

Holo typ e.

Slide 453/2 39.5 102.6 Illustrations - PI. 22 figs. 3,4.

(37 microns). - 179-

Remarks .

The exoexinal sculpture of specimens assigned to Cirratri- radites buZgoensis sp. nov. varies from finely foveolate to distinctly reticulate. There is a complete gradation between the end members of this morphological series.

C omp ar is ons.

Cirratriradites megaspinosus (Ibrahim) Smith & Butterworth is superficially similar to finely foveolate specimens of

C. buZgoensis sp. nov. but is distinguished by the discrete distal spines.

Occurrence.

Cirratriradites buZgoensis sp. nov. first appears in the lower portion of the Tuggerah Formation and is known to extend almost to the top of the Patonga Formation.

Suprasubturma PSEUDOSACCITRILETES Richardson 1965.

Genus ENDOSPORITES Wilson & Coe 1940.

1932 Sporonites (partim.J, Ibrahim (in Potonie, Ibrahim & Loose),

p . 4 4 7 .

1933 Zonales-sporites Bennie & Kidston (partim.), Ibrahim, p.28.

1940 Endosporites Wilson & Coe, p. 184.

1954 Guthoerlisporites Bharadwaj, p. 518.

Type species. Endosporites gZobiformis (Ibrahim) Schopf, Wilson

& Bent all

Although Wilson & Coe (1940, p. 184) designated Endosporites ornatus Wilson & Coe as' type species of Endosporites _, Helby

(1966, p. 671) suggested that E. ornatus is a junior synonym of E. gZobiformis (Ibrahim) Schopf, Wilson and Bentall. Professor - 180-

Wilson (pers. comm.) disputes this.

Remarks .

Bharadwaj (1954) proposed Guthoerlisporites as a taxon

similar in organisation to Endosporites Wilson & Coe 1940, but

differing from it durch starke Faltung des Zentralkorpers,

kürzere tecta und die Abwesenheit eines Limbus oder einer

äquatorialen Verdickung des Saccus" (Bharadwaj 1954, p. 519).

Potonie (1958, p. 40) suggests that the genus is not satisfac

torily delineated from Wilsonites Kosanke 1959. Playford &

Dettmann (1965, pp. 146-147) also comment on the "highly sub

jective" nature of Bharadwaj’s differential diagnosis, indicat

ing the obvious necessity for re-examination of the type species

of Wilsonites Kosanke 1959, Remysporites Butterworth & Williams

1958 and Guthoerlisporites Bharadwaj 1954. I have examined the

holotype of Guthoerlisporites magnificus Bharadwaj and consider

it to be indistinguishable from the Endosporite s globiformis

population in the type material, and in topotype material which

I have previously described (Helby, 1966). I regard Guthoer

lisporites as a junior synonym of Endosporites.

Playford & Dettmann (1965) have tentatively accepted

Guthoerlisporites interpreting it broadly to accommodate trilete,

distinctly acavate (with a wide gap between intexine and exoexine

in equatorial and distal regions) microspores, the exoexine of which is finely but regularly reticulate. Balme (1969) has

commented that the exoexine of the species assigned to Guthoer

lisporites by Playford & Dettmann (G. canc ellatus Playford &

Dettmann 1965) is actually intrareticulate. Apart from the - 181-

extreme ly regular nature of the exoexinal intrareticulation, which I am not prepared to accept as a character of generic

significance at this stage, these forms conform to Endosporites.

Endosporites radiatus (Hennelly) comb. nov.

PI. 2 4 figs. 1 - 6

Selected Synonymy.

1953 Type 34c, Taylor p. 161, p. 162 fig. 34c.

1958 Nuskoisporites radiatus Hennelly, p. 366, pi. 5 figs.10-12.

1965 Guthoerlisporites oanoellatus Playford & Dettmann, p. 147,

pi. 14 figs. 33 - 35.

Description of specimens.

See Playford & Dettmann (1965, p. 147)

Dimens ions.

Exoexine diameter 92 (107) 138 microns.

Intexine " 43 (57) 66 microns.

25 specimens measured from sample 1006.

Exoexine diameter 62 - 138 microns - specimens ranging

from base of Narrabeen Group to top of Wianamatta Group.

Comp a r i s ons.

As previously indicated by Balme (1970 p. ), E . radiatus

(Hennelly) comb. nov. is difficult to delineate from E. velatus

Leschik and E. hexareticulatus Klaus. Playford & Dettmann

suggest that E. velatus Leschik can be distinguished by

its granulate exoexine, although, Potonie (1958, p. 40) suggests

that this species be assigned to Guthoerlisporites, which may

imply he interprets this species as having an intrareticulate ornament. E. hexaretioulatus Klaus has a slightly larger size 182- range and possible wider intrareticulate lumens than E. radiatus

(2 microns), although these characters scarcely rank as diagnos tic. Several specimens from the Early Permian Wellington

Formation of Oklahoma (illustrated by Hedlund 1965, pi. 2 figs. 6, 7) are difficult to distinguish from E. radiatus

(Hennelly) comb. nov. Forms described by Wilson (1962) as

Nuskoisporites orenulatus may be similar.

Remarks.

Hennelly (1958, pi. 5 figs. 10, 12) illustrated several specimens of Endosporites radiatus in which the proximal surface of the exine was peeled back along the laesurae. This feature is relatively common in basal Narrabeen Group populations but is extremely rare in higher parts of the section. Hennelly indicates that exoexine intrareticulation exhibits lumens up to

2.5 microns diameter. Lumen diameter in the specimens examined here varied from 1 - 2 microns.

Previous records.

Spores referable to E. radiatus have previously been reported from Upper Permian basal Narrabeen Group microfloras in the Sydney Basin (Hennelly, 1958). Taylor (1953) and Playford

& Dettmann (1965) have identified it at Leigh Creek, South

Australia where it appears to be confined to Triassic sediments.

It ranges from the Ross Formation to the Brady Formation in north-eastern Tasmania (Playford, 1965). De Jersey (1968) reports its occurrence in the Clematis Sandstone of eastern

Queensland, although not from the Moolayember Formation. Balme

(1970) has documented its range as extending from uppermost - 183-

Permian to Lower Triassic in the Salt Range succession. Extrem ely similar forms have been reported from the Upper Permian

Zechstein Group of Germany (Endo sporite s velatus Leschik) and in the Upper Permian Groedner Sandstone and Bellerophon Beds of the Dolomites in Southern Europe (Endosporites hexareticulatus

Klaus).

Occurrence.

Endosporites radiatus (Hennelly) comb. nov. first appears as a relatively common component of basal Narrabeen microfloras.

It is not encountered in typical Upper Permian Coal Measure assemblages. It ranges through the Narrabeen Group, Hawkesbury

Sandstone, Wianamatta Group and their equivalents.

Turma MONOLETES Ibrahim 1933

Infraturma LAEVIGATOMONOLETES Dybova & Jachowicz 1957

Genus LAEVIGATOSPORITE S Ibrahim 1933

Type species. Laevigatosporites vulgaris Ibrahim - original

des igna t io n .

Laevigatosporites vulgaris (Ibrahim) Ibrahim

PI. 25 fig. 36.

1932 Sporonites vulgaris Ibrahim (in Potonie, Ibrahim & Loose)

p. 448, pi. 15 fig. 16.

1933 Laevigatosporites vulgaris (Ibrahim) Ibrahim, p, 39, pi. 5

figs. 37-39.

Occurrence.

Laevigatosporites vulgaris was encountered in microfloras taken from the horizon of the Vales Point Coal Member. It is recorded intermittently from basalmost Narrabeen Group micro floras (lower zonule of the Protohaploxypinus reticulatus - 184-

Assemblage Zone) in which it occurs as an extremely rare

microfloral component.

Infraturma SCULPTATOMONOLETES Dybova & Jachowicz 1957

Genus PUNCTATOSPORITES Ibrahim 1933

Type species. Punotatosporites minutus - by original monotypy.

Punotatosporites sp. cf. P. walkomi de Jersey

See Plate 25.

1962 Punotatosporites walkomi de Jersey, p. 6, pi. 2 figs. 6,7.

Remarks.

Specimens assigned to this category are only tentatively

compared with Punotatosporites walkomi de Jersey. I have con

siderable difficulty in satisfactorily distinguishing the con

cepts of P. walkomi and P. minutus Ibrahim. These forms also

display an uncomfortably close similarity to Tuberculatosporites abadarensis de Jersey, the implication being that they are

preservation variants of that species (or vice versa taking

priority into account).

Previous records.

Forms assigned to Punotatosporites walkomi are reported widely from the Triassic of Queensland (de Jersey 1962, 1964,

1968; de Jersey & Hamilton 1967, 1969). Playford (1965) records

this form as a common component of Mid and Late Triassic micro

floras of northern Tasmania, while Playford & Dettmann (1965)

record it's occurrence in the Triassic portion of the Leigh

Creek Coal Measures. Its occurrence in Lower to Mid Jurassic microfloras of the Surat Basin is recorded by Paten (1967) and

Reiser & Williams (1969).

Occurrence.

Punotatosporites sp. cf. P. walkomi occurs intermittently - 185- throughout the Narrabeen Group, Hawkesbury Sandstone, Wianamatta

Group and their equivalents. Because of existing doubts con cerning its identification it has often been assigned to Seulpta- tomonoleti indet. on the range tables.

Genus TUBERCULATOSPORITES Potonie & Kremp ex Ingrund 1960.

Type species. Tuberculatosporites anioystoides Potonie & Kremp

ex Imgrund - original designation.

1954 Tuberoulatosporites nom. nud. Potonie & Kremp, p. 166, pi.16

f ig . 70 .

1960 Tuberoulatosporites Potonie & Kremp ex Imgrund, p. 176

Remarks.

Despite the arguments of Potonie (in Imgrund, 1960, p. 145) it is difficult to accept that Imgrund's original thesis was published. This being the case the genera which Potonie & Kremp

1954 ascribe to Imgrund lack validly erected type species.

These genera and the type species assigned to them are therefore regarded as taxa of the nomen nudem category, with Potonie &

Kremp as the publishing authors. Tuberoulatosporites was sub sequently validated by publication of the description and illu strations of T. anicystoides by Imgrund (1960).

Spinosporites Alpern 1958 is similar in concept to Tuber oulatosporites and would have precedence over it. However, the holotype of S. spinosus Alpern does not clearly exhibit a mono- let e mark.

Tuberoulatosporites abadarensis de Jersey

PI. 25 f igs. 1-5 .

1964 Tuberoulatosporites abadarensis de Jersey, p. 8, pi. 1

figs. 17. 18. - 186-

Description of specimens.

Microspores, monolete. Amb oval to circular. Laesura usually

distinct, often bordered by irregularly thickened, occasionally

sculptured labrae, extend 2/3 to almost full length of spore.

Exine 1-2 microns thick, not noticeably layered, bearing spines

(1.5 - 4 microns in length, 0.5 - 2 microns basal diameter)

coni (1-2 microns basal diameter, 1.5-2 microns high) and

occasionally small irregular verrucae. Bases of sculptural

elements occasionaly merge to form sculptured rugulae. Sculp

tural elements irregularly spaced from less than 0.5 -.2.5 microns apart.

Dimens ions.

Long axis 20 (25) 33 microns. 20 specimens measured.

Remarks.

There is a definite tendency for the spines of this species to be reduced by maceration. The end product of this process is a grain which could be assigned to Punotato sporites walkomi de

Jersey.

Previous records.

Tuberoulatosporites abadarensis is identified with certainty only in microfloras from the Bundamba Group (de Jersey 1964).

However, tentative identifications of this species are recorded from the Moolayember Formation. Unspecified Tuberoulatosporites forms are reported from Wandoan Formation (de Jersey & Hamilton,

1969) the Clematis Sandstone (de Jersey, 1968) and the Tingalpa and Moorooka Formations of southern Queensland (de Jersey &

Hamilton, 1965 a, b.) - 187-

Occurrence .

Tubereulatosporites abadarensis extends throughout the

Narrabeen Group, Hawkesbury Sandstone, Wianamatta Group and

their equivalents. It attains maximum prominence in samples from

the Wianamatta Group and equivalents.

Genus POLYPODIISPORITES Potonie & Gelletich ex Potonie 1956

Type species. Potypodiisporites favus Potonie - designated

by Potonie (1956, p. 78).

Remarks.

A comprehensive review of the development of the concept

of Potypodiisporites and its validity relative to other genera

of similar morphology is contained in Potonie (1956, p. 78) and

Playford & Dettmann (1965, p. 150).

Potypodiisporites sp. cf. P. eicatrieosus (Balme & Hennelly) comb. nov.

PI. 25 fig. 31

1956a Verrucos osporitzs eicatrieosus Balme & Hennelly, p. 57,

pi. 1 figs. 14-18.

1956b Thymospora eicatrieosus (Balme & Hennelly) Hart, p. 120,

text f ig. 298.

Remarks.

The precedence of Potypodiisporites Potonie & Gelletich ex Potonie 1956 over Thymospora Wilson & Venkatachala 1963 has been established by Playford & Dettmann (1965).

The specimens assigned to P. sp. cf. P. eicatrieosus conform closely to the type population of P. eicatrieosus

(Balme & Hennelly) comb. nov. However, Balme & Hennelly recovered this species only from Lower Permian coals of the - 188-

Greta Coal Measures. Evans (1970, fig. 4) suggests that this species scarcely extends beyond the lower limit of Stage 5

(possibly low Mid Permian equivalent). It lacks the spinose projections which characterise Polypodiisporites hamatus (Balme

& Hennelly).

Holotype .

Although Balme & Hennelly (1956a, p.57) indicated the Greta

Seam as type locality of this species a holotype was not assigned.

Subsequently, Hart (1965b, p.120) selected the specimen illus trated by Balme & Hennelly (1956a, PI. 1 fig. 14) as "holotype"

( = lec to type) .

Occurrence.

This species was identified from the lower zonule of the

Protohaploxypinus retioulatus Assemblage Zone in the Terrigal

No. 1 well, in Newvale D.D.H. No. 28 (immediately above the

Vales Point Coal Member) and the lowermost Wollar Sandstone at the Cox’s Gap tunnel (Protohaploxypinus retioulatus Assemblage

Zone). Assuming the known range of Polypodiisporites oioatricosus as shown by Evans (1970) to be correct, these grains are inter preted as evidence of recycling of Lower - Mid Permian sediments.

Polypodiisporites hamatus (Balme & Hennelly) comb. nov.

PI. 25 figs. 26, 27

1956a Verruoososporites hamatus Balme & Hennelly, p. 57, pi. 1

f igs. 19-21.

1965b Thymospora hamatus (Balme & Hennelly) Hart, p. 120,

text fig. 299.

Remarks.

The distinction between Polypodiisporites hamatus (Balme & - 189-

Hennelly) comb. nov. and P. oioatrioosus CBalme & Hennelly) comb. nov. appears to be based on the occurrence of discrete spinose sculptural elements in the former species. However, this distinction is not universally applicable. The specimen illustrated on pi. 25 figs. 26, 27 displays distinct spinose elements, which sometimes bifurcate, surmounting a basic rugulate ridge (3-4 microns across) system.

Holotype .

Although Balme & Hennelly (1956a, p. 57) indicated a type locality a holotype was not allocated. Subsequently, Hart

(1965b, p.120) has selected the specimen illustrated by Balme

& Hennelly 1956a,PI. 1 fig. 19 as "holotype" (= 1ectotype) .

Previous records.

Balme & Hennelly (1956a, p.57) indicated that this species has been identified in the Tomago and Newcastle Coal Measures of the Sydney Basin {Dulhuntyispora Assemblage Zone).

Occurrence.

Several specimens referrable to Polypodiisporites hamatus

(Balme & Hennelly) comb. nov. were encountered as very rare components of the Dulhuntyispora Assemblage and in assemblages of the lower zonule of the Protohaploxypinus reticulatus Assem blage Zone .

Polypodiisporites ipsvioiensis (de Jersey) Playford & Dettmann.

PI. 25 figs. 12-14, 16-20.

Selected Synonymy.

1962 Verrucososporites ipsvioiensis de Jersey, p. 7, pi. 2

f igs. 8-10 . - 190-

1965 Polypodiisporites ipsviciensis (de Jersey) Playford &

Dettmann, p.150, pi. 15 figs. 39,40

1968 Thymospora ipsviciensis (de Jersey) Jain, p.15, pi. 2

figs. 29. 30.

Description of specimens.

See Playford & Dettmann.

Remarks.

Playford & Dettmann (1965) have interpreted Polypodiisporites ipsviciensis to include a broad range of sculptural variation.

The full limites of this variation are recognised in the Sydney

Basin material. I have observed that the size of the sculpt ural elements gradually increases up the section. It is, however, not possible to divide the populations on this basis.

Comp arisons.

Polypodiisporites ipsviciensis closely resembles some' specimens of Leschikisporis mutabilis (Balme) comb. nov. This latter form is distinguished by the tendency to develop three laesurae and generally displays considerable variation of sculpture. Polypodiisporites sp. cf. P. cicatricosus (Balme

& Hennelly) comb. nov. is distinguished by its distal, irregu larly thick, sinuous ridges which often disply a number of sharp projections (not actually spines).

Occurrence.

Polypodiisporites ipsviciensis occurs throughout the

Narrabeen Group, Hawkesbury Sands tone,Wianamatta Group and their equivalents. It is a fairly constant but seldom common component of the microfloras in which it occurs. - 191-

Sup ras ub turma CAVATOMONOLETES Smith & Butterworth 1967.

Genus ARATRISPORITES Leschik emend. Playford & Dettmann 1965

Selected Synonymy.

1949 Poltenites (partim.) Thiergart, p.12

1955 Aratrisporites Leschik, p. 38.

1960 Aratrisporites Leschik emend. Klaus, p. 145

1960 Saturnisporites Klaus, p. 142

1962 Zonomonotetes Luber (partim.) - Tschalyschev & Varyukhina, pi. 3 fig. 13 ?1962 Todites Kurbatova p.30, pi. 2 figs. 11,12.

1964 Aratrisporites Leschik emend. Bharadwaj & Singh, p. 36

1965 Aratrisporites Leschik emend. Playford & Dettmann, p. 151

Type species. Aratrisporites parvispiviosus (Leschik) Playford

- original designation.

Remarks.

Since Leschik's original interpretation of Aratrisporites

(Leschik, 1955) which included alete, zonate, sculptured (usually

echinate) microspores, the concept of the genus has been con

stantly evolving. Potoniè (1958, p. 84) accepted the genus as

alete, but inferred (by reference to a saccus) that the exine

may have been cavate. Klaus (1960) recognised the monolete

nature of Aratrisporites 3 and in emending the genus interpreted

it as zonate and acavate (see Klaus 1960, text figs. 8, 9).

Illustrations of A. saabratus Klaus 1960 (pi. 32 figs. 37 and

perhaps 38) clearly exhibit the cavate nature of the exine in

that form. Klaus (1960) also proposed a new genus - Saturni-

sporite s j to accommodate forms which differed from Aratrisporites

only marginally in the relative prominence of the monolete mark - 192- and in curling of the lateral exoexine extremities of Aratri sporites. The majority of later authors have regarded these taxa as synonymous. Klaus (1960) also established the lycoposid affinities of Aratrisporites by comparison with microspores extracted from Lyeostrobus scotti Nathorst. Despite this,

Bharadwaj & Singh (1964, p. 36) in proposing an emendment of the genus interpret it as an alete, monosaccate form and assign it to the Aietisaeciti (Anteturma Pollenites). Maedler (1964) although accepting Klaus’ emendation of Aratrisporites recognises the cavate nature of the exine, referring to the partially detached intexine as a "mesospore". Most recently Playford &

Dettmann (1965) have emended the genus to encompass, monolete, cavate microspores with a sculptured exoexine. These authors reject Klaus’ zonate interpretation. Many later authors (Balme,

1970; de Jersey & Hamilton, 1967; Helby, 1967) have followed the Playford & Dettmann emendation.

On the basis of presently available information it may be suggested that Aratrisporites is an important biostratigraphic form. Helby (1967) has indicated that it first appears in upper most Scythian sediments at widely scattered localities, attaining some prominence in the Mid Triassic. It ranges into the Late

Triassic and there are no confirmed reports of its occurrence in younger sediments. Unfortunately, a rash of species has been assigned to Aratrisporites (presently in excess of 25), fourteen of which are reported from eastern Australian localities. In the Sydney Basin succession I recognise four broad species, which are most closely associated with - - 193-

1. Aratrisporites ooryliseminis Klaus

2. Aratrisporites granulatus (Klaus) Playford & Dettmann

3. Aratrisporites parvispinosus Leschik emend. Playford

4. Aratrisporites tenuispinosus Playford

Prompted by the extreme diversity of morphology in indi

vidual species populations of Aratrisporites in the study

material I have made a number of general observations -

1. Not all representatives of Aratrisporites are necessarily

cavate. Cavate and acavate exoexinal conditions can exist in

a single population (see A. wollariensis - Helby, 1967). A

cavate exinal organisation can definitely be accentuated and

possibly even initiated by oxidation processes during sedimen

tation and subsequent weathering and or preparation treatment.

Similar circumstances have been discussed by Playford & Helby

(1968) in relation to "Kraeuselisporites" kuttungensis Playford

& Helby.

2. The exoexine of most species of Aratrisporites is extremely

sensitive to oxidation. It first swells, becoming thicker but

less dense and gradually loses the outer sculptured surface by

reduction of the individual elements. The intexine of most

species is relatively resistant to oxidation.

3.Some forms are both cavate and incipiently zonate, although

"pseudozonate" (closely pressed double layer of exoexine) are more common, particularly in samples which have not been oxidised.

Aratrisporites ooryliseminis Klaus

PI. 26 figs. 1-8

Selected Synonymy.

1960 Aratrisporites ooryliseminis Klaus, p. 147, pi. 33 figs. 34, 40. MEASUREMENT PLAN OF ARATRISPORITES.

A Length of exoexine B Breadth of exoexine C Length of intexine D Breadth of intexine - 194-

1965 Avatrispovites banksi Playford, p.144, pi.10 figs. 11-14,

pi. 11 figs. 1, 2.

1967 Aratrisporites plioatus de Jersey & Hamilton, p. 13, pi. 7

figs. 1 - 3

Description of specimens.

Microspores, inonolete, usually cavate, sometimes zonate.

Amb spindle shape to oval (becomes more oval shaped with worsen ing preservation), distal surface markedly inflated, proximal surface usually arched along monolete mark. Shape boat like in compressions slightly oblique to the proximo-dista1 plane.

Laesura usually straight, extending to the lateral limits of the exoexine. In some cases (pi. 26 fig. 8) the laesura extends beyond the extremity of the intexine on a thickened exoexinal keel. Laesura usually accompanied by raised lips. Exine two layered, distinctly cavate. Exoexine 1.5 - 2.5 microns thick, spongeous with an irregular sponge like surface expression. In specimens which possess extremely coarse exoexine structure, small irregular spines are developed. Shallow folds often simu late an imperfect reticulum. Exoexine often delineated into a narrow zona in the equatorial regions. Zona usually projects in the proximal direction. Intexine apparently smooth.

Dimens ions.

A 55 (73) 99 microns - 25 specimens measured from sample 530.

B 40 (48) 57 microns

C 43 (55) 68 microns

D 29 (35) 44 microns

Exoexinal length from total populations varies from 38 - 126

microns . 195-

Remarks .

The forms listed in the synonymy above are all characterised by a spindle like shape, a thick, distinctly spongeous exoexine which may or may not have integral spines developed and a lipped laesura which extends to the edge of the amb. Taking into account the apparent significance of size variation and the effect of oxidation processes on the type of microspore, I do not believe that I can satisfactorily delineate the synonymised species.

Microspores similar to A. ooryZiseminis have been extracted from an undescribed CyZostrobus fructification collected from Avalon

Beach, Sydney. They are associated with a very large megaspore

(1.2 - 2 mm) referrable to Banksisporites Dettmann 1961.

C omp ar is ons.

Aratrisporites ooryZiseminis Klaus is distinguished from

A. parvispinosus (Leschik) Playford by the irregular sponge like surface of the exoexine, the absence of discrete spines and its shape in polar and lateral views. It differs from A. granuZatus

(Klaus) Playford & Dettmann in the external appearance of the exoexine and the extension of the laesura across the exoexinal extremities. A. erassiteotatus Reinhardt would appear to have a finely spongeous exoexine, although Reinhardt (1964, p. 54) states that the exine is punctate.

Occurrence.

Aratrisporites ooryZiseminis Klaus first appears in the

Upper part of the Bulgo Sandstone and its equivalents throughout the Sydney Basin. It is intermittently abundant in the upper portion of the Narrabeen Group and the Hawkesbury Sandstone, - 196-

becoming less prominent in Wianamatta Group sediments.

Aratrisporites granulatus (Klaus) Playford & Dettmann

PI. 26 figs. 9-14, PI. 27 figs. 1-4

Selected Synonymy.

1960 Saturnisporites granulatus Klaus, p. 143, pi.32 fig. 34.

? 1964 Aratrisporites saturni (Thiergart) Maedler, p. 184, pi. 9

f igs. 8-12.

1965 Aratrisporites granulatus (Klaus) Playford & Dettmann, p.152

? 1965 Aratrisporites sp. cf. A. granulatus (Klaus) Playford &

Dettmann - Playford, p. 197, pi.10 fig. 10.

Description of specimens.

Microspores, monolete, usually cavate, often zonate. Amb oval to spindle shaped, distal surface usually inflated, proximal

surface relatively flat or slightly arched along laesura. Laesura usually extends to lateral limits of intexine, often slightly

sinuous, usually accompanied by raised lips (1-3 microns high,

1-2 microns wide). Exine two layered, usually noticeably cavate.

Exoexine 1-1.5 microns thick, spongeous with a finely granulate surface, often differentiated at the equator to form narrow

(1-3 microns wide) zona (see pi. 27 figs. 1, 2). Intexine smooth, about 0.5 microns thick.

D imens ions.

A 31 (43) 55 microns - 25 specimens measured from sample 556.

B 27 (47) 48 microns

C 23 (35) 48 microns

D 17 (28) 39 microns

Remarks.

The presence of the zona is best exhibited by specimens - 197- comp ressed in planes slightly oblique to the proximo-distal plane. Exoexine and intexine are almost invariably in contact along the monolete mark.

Comparisons. TT The specimens described above are indistinguishable from forms described by Klaus (1960) as Satuvnispovites granulatus.

Aratvispovites granulatus is distinguished from most species of

Avatvispovites reported from Australian localities by the absence of spines. It is somewhat similar to specimens referred to A. covyliseminis Klaus by Playford & Dettmann (1965, p. 153, pi. 15 figs. 41-43) but differs in its exoexinal surface pattern.

Occurrence.

Aratvispovites granulatus (Klaus) Playford & Dettmann first appears in the Tuggerah Formation and its equivalents throughout the Sydney Basin. It has not been encountered in sediments above the horizon of the Bald Hill Claystone.

Aratvispovites pavvispinosus Leschik emend. Playford.

PI. 27 figs. 5-15

1955 Aratvispovites pavvispinosus Leschik, p. 38, pi. 5 figs.2,4

? 1960 Aratvispovites pavaspinosus Klaus, p. 148, pi. 33 figs.

43, 44.

1962 Zonomonoletes tsohaly sohevi Varyukhina (in Tschalyschev &

Varyukhina) pi. 3 fig. 13.

1965 Aratvispovites flexibilis Playford & Dettmann, p. 153, pi.15,

f igs. 46-48.

1965 Aratvispovites paenulatus Playford & Dettmann,p. 154, pi.15

figs. 44-45. - 198-

1965 Aratvispovites parvispinosus Leschik, emend. Playford,

p. 194, pi. 10 figs. 1, 2.

1967 Aratrisporites goulburniensis Helby, p.66, pi. 1 figs.14-16.

Description of specimens.

Microspores, monolete, usually cavate. Amb oval, distal

surface originally inflated, proximal surface flat or slightly

arched along the laesura. Laesura straight or slightly sinuous,

extending to the lateral limits of the exoexine, usually

accompanied by raised lips. Exine two layered, usually notice

ably cavate. Exoexine 1 - 2.5 microns thick, spongeous with

patterned outer surface which usually has a granulate appearance.

Distinct spines (up to 6 microns high and 2.5 microns basal

diameter), and or coni (up to 3 microns high and 2.5 microns basal diameter) occur, randomly scattered but seldom close

together on exoexine. Intexine smooth about 0.5 microns thick.

Dimens ions.

Dimensions are extremely variable in most populations.

Exoexine/intexine width ratios are obviously dependant on the relative state of preservation of the material.

Remarks.

I interpret Aratrisporites parvispinosus as a fairly broad

taxon encompassing Aratrisporites forms which have a character

istic exoexine structure with a predominantly granulate surface expression and bearing discrete, widely scattered, echinate sculptural elements. All species listed in the synonymy above conform to this concept. I consider that most of the characters of these forms which are expressed as a function of size cannot - 199-

be accepted as diagnostic because of the sensitivity of the

exoexine to various processes of oxidation. It is particularly

evident that size of projecting sculptural elements is reduced

by worsening preservation or oxidation during preparation. This

process is accompanied by swelling of the exoexine. As the

intexine is relatively resistant to oxidation, the cavate nature

of the exine is gradually accentuated.

C omp ar i sons.

Aratrisporites parvispinosus differs from A. granulatus

(Klaus) Playford & Dettmann in possessing projecting sculptural

elements. Where specimens of A. parvispinosus are badly pre

served, and spines are not apparent the extension of the laesura

to the lateral edges of the exoexine and the exaggerated cavate

organisation distinguish A. parvispinosus. Aratrisporites eory-

liseminis Klaus is distinguished by the irregular, sponge like

surface of the exoexine, and indistinct nature of the spines.

A. ooryiiseminis also maintains a more spindle like shape and

is characterised by proximal curling of the lateral exoexine.

Occurrence.

Aratrisporites parvispinosus Leschik emend. Playford first appears in the Hawkesbury Sandstone and its equivalents in the

Sydney Basin. It extends throughout the Wianamatta Group in

intermittent abundance.

Aratrisporites tenuispinosus Playford

PI. 25 figs. 29, 32-34, 37-39.

Selected Synonymy.

1965 Aratrisporites tenuispinosus Playford, p.196, pi.11 figs.3-7 - 200-

1965 Aratrisporites strigosus Playford, p.195, pi.10 figs.6-9

1967 Aratrisporites wollariensis Helby, p.67, pi. 1 figs.17-19

1967 Aratrisporites sp. - Helby, p. 68, pi. 2 fig. 20.

1968 Aratrisporites tenuispinosus Playford - de Jersey,

p. 11, pi. 5 fig. 8 (not fig.9 as indicated).

Description of specimens.

Microspores, monolete, cavate. Amb oval to elliptical,

distal surface originally inflated, proximal surface more or less

flat. Laesura straight or slightly sinuous, extending full

length of intexine, often accompanied by slightly raised lips.

Exine two layered, usually noticeably cavate. Exoexine varied

from 0.5 - 1.5 microns thick (dependant on state of preservation),

covered by scattered spines 1-3 microns apart. On well preserved

specimens, spines up to 5 microns in length, 0.5 - 1.5 microns basal diameter, tapering gradually to the tip. Spines usually

larger on distal and equatorial surface, diminishing in size on proximal surface approaching the apex. Exoexine between spines usually smooth. Intexine smooth, about 0.5 microns thick.

Dimens ions.

A 29 (42) 58 microns - 20 specimens measured from sample 764.

B 27 (33) 42 microns

C 24 (38) 44 microns

D 20 (27) 37 microns

Remarks.

I consider that forms previously described as Aratrisporites tenuispinosus Playford, A. strigosus Playford and A. wollariensis

Helby comprise a continuous morphological series. The inter relationship of specimens assignable to these species is illus- - 201- strated on pi. 25. The only definitive criterion which can be applied to distinguish these forms is the relative length of the spines. The relationship of sculpture development of microspores to the physiological history of the parent plant has scarcely been investigated in modern plants so that interpretation of this relationship in fossil material is obviously premature. However,

I have no doubt that the growth environment of the parent plant has considerable influence on variations in size of the spore and relative development of the sculpture. These variations can be observed at population level from sample to sample. As stated above most species of Aratrisporites are particularly sensitive to oxidation. This is most evident in the wide range of pres ervation states of A. tenuispinosus, resulting in breaking of spines and/or their gradual reduction by the above process, usually as a result of weathering of the sediment.

It is also possible that these forms are representative of a polyspecial parent group. Microspores, indistinguishable from

A. tenuispinosus have been extracted from a number of species of the lycopsid fructification, Cylostrobus Helby & Martin 1965, where they are associated with megaspores referrable to Banksi- sporites Dettmann 1961. Helby (1967, p. 68) has suggested that forms described as A. wollariensis had possible affinities with the megaspore Nathorstisporites puleherrima Helby. However, A. parvispinosus Leschik emend. Playford (=A. goulburnensis Helby) occurred in the same assemblage, so that the relationship suggested by Helby remains uncertain.

Comparisons.

Aratrisporites tenuispinosus differs from A. granulatus -202

(Klaus) Playford & Dettmann in possessing spines. A. parvispinosus Leschik emend. Playford is distinguished by the dis tinctive exoexine patterns between its very much coarser spines.

Occurrence.

Aratrisporites tenuispinosus first appears at about the level of the base of the Patonga Claystone and its equivalents throughout the Sydney Basin. It extends throughout the Hawkes- bury Sandstone and Wianamatta Group and is intermittently abundant.

Anteturma POLLENITES Potonie 1931

Subturma MONOSACCITES Chitaley emend. Potonie & Kremp 1954

Genus BASCANISPORITES Balme & Hennelly 1956.

Type species. Baseanisporites undosus Balme & Hennelly -

original designation.

Remarks.

I consider Baseanisporites to be distinguished from Para- saeeites Bharadwaj & Tiwari 1964 by the fine infrareticulation of the saccus exoexine and the irregular (almost polysaccate) outline of the saccus. It differs similarly from Nuskoisporites

Potonie & Klaus 1954 and Cordaitina Samoilovitch 1953.

Baseanisporites undosus Balme & Hennelly

PI. 28 figs. 7 , 8.

1956b Baseanisporites undosus Balme & Hennelly, p. 256, pi. 10

figs. 81-83

Description of specimens.

See Balme & Hennelly 1956b, p. 256.

Holotype.

Although Balme & Hennelly (1956b, p. 256) designated the - 203-

seam at 688 ft., South Wallarah D.D.H. No. 2 as the type locality

no holotype was assigned. Hart (1965b, p. 95) has proposed the

specimen illustrated by Balme & Hennelly 1956b, pi. 10 fig. 81

be accepted as lectotype.

Previous records.

Bas oanisporites undosus appears to be confined to the

Late Permian in Eastern Australia (Evans in press). It has

recently been reported from a probable Late Permian microflora

recovered from the Amery Formation, Antarctica (Balme & Playford,

1967 ) .

Occurrence.

Basoanisporites undosus Balme & Hennelly occurred as a

rare component of microfloras between and including the Vales

Point Coal Member and the Wallarah Seam in Newvale D.D.H. No. 28.

Genus STRI0M0N0 SACCITE S Bharadwaj 1962

Type species. Stv'iomonosaco'ites ovatus Bharadwaj - original

des igna t ion.

Remarks.

Bharadwaj (1962 pp. 87, 88) proposed two form genera to

accommodate striate, monosaccate pollen. The concept of Strio- monosaooites Bharadwaj 1962 encompassed monosaccate forms with a striate cappa. As defined, Distviomonosacc'ites Bharadwaj

1962 displayed both striate cappa and cappula. The distinction between the type species of these genera was not clearly illus

trated and Bharadwaj did not comment on the morphological rela

tionship of these forms to elements of diverse and dominant

Striatiti component of the Raniganj microfloras. - 204-

There is a tendency among many of the Permian-Lower Triassic

striate bisaccates towards complete equatorial detachment of the

exine layers, resulting in distinct monosaccate organisation.

The distribution of some of these forms in the Sydney Basin

succession suggests that there may have been an environmental

control in their development. The occurrence of this type of

grain is usually rare, but it is noted that they are invariably

associated with bisaccate grains exhibiting essentially similar

cappa organisation.

Stviomonosaooites movondavensis Goubin

PI. 28 fig. 9, pi. 30 fig. 3.

1965 Stviomonosaooites movondavensis Goubin, p. 1421, pi. 1

figs. 5, 6.

Description of specimens.

Pollen, monosaccate, usually striate. Amb extremely variable, usually sub-circular. Shape of intexine difficult

to determine due to coarse exoexine structure. Cappa, striate,

sub-circular in shape, usually developed over 1/2 to 2/3 diameter

of the grain. Cappa divided into 8-15 poorly defined, closely

packed (0.5 - 1 micron apart), often branching or discontinuous

striae. In very small percentage of the specimens the cappa is

restricted, occurring as a small (1/4 to 1/3 radius), non striate

disc of structured exoexine. Cappa striae finely infrareticulate.

Cappula of similar shape and dimensions to cappa, smooth exoexine but obviously structured) to finely infrareticulate. Saccus

exoexine coarsely infrareticulate.

Dimens ions.

Overall diameter 96 (128) 193 microns. 100 specimens - 205- measured from samples 634 and 641.

Remarks.

Although the specimens assigned to Strdomonosacedtes moron- dav ensds Goubin form a continuous morphological series with

Protohaploxypdnus mderocorpus (Schaarschmidt) Clarke 1965 they are a characteristic and prominent component of the Lunatispordtes pelluoddus Assemblage. The stratigraphic significance of these forms has prompted me to delineate them as a separate species.

0 c c ur r enc e.

Strdomonosaeedtes morondavensds Goubin occurs as a very rare component of basal Narrabeen Group microfloras. It attains wide spread abundance in association with Lunatdspordtes pellu oddus (Go ub in) Conib. no^in upper part of the Munmorah Congolmerate, the Stanwell Park Claystone and the lowermost Grose Sandstone.

Genus CRUSTAESPORITES Leschik 1956

Type species. Crustaespordtes globosus Leschik - original

designation.

Remarks.

Leschik (1956, p. 130) instituted Crustaespordtes to accommodate striate pollen with three sacci. The illustration of the holotype of C. globosus Leschik (1956 pi. 21 fig. 2) suggests that this form is probably a freak bisaccate grain.

Jansonius (1962, p. 52) has reinterpreted C. globosus as monosaccate, emending the concept of the genus to include essentially monosaccate forms. This emended concept is identical to that of

Strdomonosaoodtes Bharadwaj 1962. Crustaespordtes could be - 206- regarded as invalid if the holotype of the type species is accepted as a freak. Similarly, I believe that most species

assigned to Striomonosac cites probably exhibit morphological gradation to established bisaccate species. However, as these forms occur rarely, but consistently, in the Lunatisporites

pellucidus Assemblage Zone they should be delineated, at least until their stratigraphic significance is determined.

Crustaesporites sp.

PI. 29 figs.1-4.

Description of specimens.

See Balme 1963, p. 30.

Remarks.

Balme (1963, p. 30) has commented on the affinity of

Crustaesporites to the Striatiti. The specimen he illustrated

as Crustaesporites sp. (pi. 6 fig. 11) displays a marked simi larity in the organisation of the cappa and the nature of the

saccus exoexine to Protohaploxypinus microcorpus (Schaarschmidt)

Clarke, (illustrated by Balme as "Striatites sp. cf. Taeniae-

sporites antiquus Leschik" - Balme 1963, pi. 6 fig. 13). Forms

assigned to Crustaesporites sp. fill an intermediate position in a continuous morphological series between P. microcorpus

and specimens assigned to Striomonosaccites morondavensis Goubin.

Forms with three distinct, separated sacci are relatively rare and are regarded as definite freaks.

Occurrence.

This form occurs very rarely throughout the lower portion of the Narrabeen Group. It is slightly more common in association - 207- wit h abundant Striomono saccites morondavensis Goubin and

Protohaploxypinus microcorpus (Schaarschmidt) Clarke.

Subturma DISACCITES Cookson 1947

Infraturma STRIATITI Pant 1954

Genus LUECKISPORITES Potonie & Klaus emend. Leschik 1959.

Type species. Lueckisporites virkkiae Potonie & Klaus

original designation.

Selected Synonymy.

1953 Lueckisporites (nom. nud.) Klaus, p. 54.

1954 Cedripites Zoritscheva & Sedova, pi. 10 fig. 7.

1954 Lueckisporites Potonie& Klaus, pp. 531-534, pi. 10 fig. 3

text f igs. 5, 6.

1958 Lueckisporites Potonie & Klaus emend. Potonie (partim. ) , p . 50 . 1959 Lueckisporites Potonie& Klaus emend. Leschik, p. 68.

1962 Lueckisporites Potonie& Klaus emend. Jansonius, p. 60.

1963 Lueckisporites Potonie& Klaus emend. Klaus, pp.299-301.

Remarks.

The holotype of the type species (pi. 20 fig. 3) and the text figures of Lueckisporites presented by Potonie & Klaus

(1954, text figs. 4 & 5) clearly shows a single cleft dividing the prominent cappa (Kalotte). However, the interpretation given in the generic diagnosis is considerably broader "Es ist besonder kennzeichnend, dass diese Kalotte mindestens eine - und dann den proximalen Pol durchlaufende - zuweilen aber auch mehrere und dann einander - parallel verlaufende ExoexinenaufSpaltungen auf weist." This broad interpretation was widely accepted and re sulted in a large assortment of the Striatiti being referred to - 208-

Lueckisporites. Leschik (1955, p. 58 and 1956, p. 134) pro tested that Lueckisporites should be confined to forms with a single cleft. Leschik (1959, p. 60) later indicated the poten tial stratigraphic implications of the genus Lueckisporites and formally reinterpreted it as being confined to forms with a single cleft on the cappa, Jansonius (1962, p. 60) proposed a similar reinterpretation. Klaus (1963, pp. 299-301) presents a comprehensive history of Lueckisporites and a further, extrem ely thorough circumscription of the genus. Balme (1970, p. ) has reviewed the stratigraphic occurrences of the genus and it would appear that it ranges from Early Permian possibly into the

Early Trias s ic .

Lueckisporites nyakapendensis Hart

PI. 28 figs.1-3

Selected Synonymy.

1946 ?Spore 5 Virkki, p. 108, pi. 1 fig. 5.

1946 ?Spore 64 Virkki, p. 124, pi. 5 fig. 55, text fig. 33.

1960 cf. Lueckisporites nyakapendensis Hart, p. 9, pi. 1 figs.

11, 12.

1964 Lueckisporites nyakapendensis Hart 1960; Hart, p. 1177,

text fig. 46.

Description of specimens.

Pollen, bisaccate with two prominent proximal taeniae.

Outline dipo1xy1onoid. Corpus oval in polar view, b.c. greater than l .c . Taeniae almost semi-circular in shape, inner margins more or less straight and parallel to each other. Outer margin of taeniae often slightly overlaps the corpus. Cleft between MEASUREMENT PLAN OF ElSACCATE GRAINS

O.L. Overall length of grain. B.C. Breadth of corpus L.C. Length of corpus D.C. Depth of corpus B . S . Breadth of saccus L. S . Length of saccus D. S. Depth of saccus - 209-

taeniae varies up to 5 microns wide, intexine visible, thin.

Exoexine of taeniae thick (2-3 microns), finely intrareticulate.

Sacci large, roughly semi-circular to crescentic in polar view.

They project beyond the edge of the corpus equatorially . Distal

zone of saccus exoexine detachment always prominent, defining

a relatively wide cappula. Sacci display a slight distal incli

nation.

Dimensions.

O.L. 72 (83) 92 microns - 20 specimens measured from sample 591.

B.C. 57 (60.5) 70 microns

L.C. 50 (53) 63 microns

B.S. 29 (33.5) 41 microns

L.S. 49 (56) 67 microns

Remarks.

The overlap of the corpus by the taeniae suggests that the

taeniae may have been inflated prior to compression. There is

an extremely close correlation of morphology and detailed dimen

sion ranges of the forms referred above to Lueokisporites nyakapendensis Hart and the material described by Hart (1960, p. 9).

It is interesting to note that Hart regards the Tanganyika

material as Early Permian (It conforms to Balme’s "Vittatina

Assemblage"). There are, however, no published reports of

Lueokisporites in Australian Permian sediments.

Comparisons.

Clarke (1956b, p.331-333) has proposed an emendation and broader reinterpretation of Lueokisporites virkkiae Potonie &

Klaus indicating that L. microgranulatus Klaus and L. parvus - 210-

Klaus are merely end member variants of the overall morphological

range of L. virkkiae. He also assigns L. nyakapendensis Hart to

L. virkkiae synonymy. There is no doubt that L. nyakapendensis

has an essentially similar morphology to Clarke's L . virkkiae

variant A (text fig. 8). However, it differs in having a dis

tinctly elongate oval corpus and minimum size range which appears

to be in excess of the maximum dimensions of most L. virkkiae

populations published to date.

Occ urrenc e .

Lueokisp orites nyakapendensis occurs as a relatively common

component of the microfloras of samples 591, 594 & 595, in

Ourimbah Creek D.D.H. No. 5. A single specimen was identified

in sample 682 from Appin D.D.H. No. 4. All these occurrences

are confined to the lower 200 ft. of the Narrabeen Group.

Genus LUNATISPORITES Leschik emend. Maedler 1964.

Type species. Lunatisporites aoutus Leschik - original

designation.

Selected Synonymy.

1954 Lueokisporites (partim.) Potonie & Klaus, pi. 10 fig. 2.

1955 Lunatisporites Leschik, p. 56, pi. 7 figs. 21-24.

1955 Taeniaesporites Leschik, p. 58, pi. 8 figs. 1, 2.

71955 Suooinotisporites (partim.) Leschik, pi. 7 figs. 4, 5.

1958 Pollenites (partim.) Pautsch, pi. 1 fig. 8.

1962 Striatopodocarpidites Sedova, (partim.) Tschalyschev &

Varyukhina, pi. 2 fig. 10; pi. 3 fig. 16.

1962 Striatopinites Sedova, (partim.) Tschalyschev & Varyukhina,

pi. 2 fig. 13. - 211-

1963 Striatites Pant, (partim.) Schaarschmidt, pi. 14, fig. 8;

pi. 15 figs . 5-9 .

1964 Striatisaoous Maedler, p. 56.

1965 Pauoistriatoabietites Zauer, pi. 16 fig. 1

1965 Pauoistriatooonfferus Zauer, pi. 16 fig. 2

1965 Pauoistriatopinites Zauer, pi. 16 figs. 4, 5.

1966 Taeniaepollenites Visscher, p. 360.

non 1958 Lunatisporites auot. non. Leschik emend. Potonie, pp .

52, 53. non 1960 Lunatisporites auet. non. Leschik emend. Potonie

Lakhanpal et at. p. 114, pi. 1 fig. 11.

non 1960 Lunatisporites auot. non. Leschik, Hart, pi. 1 figs. 8,

14, 15.

non 1961 Lunatisporites auot. non. Leschik emend. Potonie,

Potonie & Lele, pi. 3 figs. 66-72. non 1962 Lunatisporites auot. non. Leschik emend. Bharadwaj,

text fig. 11a, pi. 14 figs. 189-192. non 1964 Lunatisporites auot. non. Leschik emend. Bharadwaj,

Bharadwaj & Salujha, pi. 10 figs. 138, 139.

Remarks.

I have examined the holotypes of Taeniaesporites kraeuseti

Leschik and Lunatisporites aoutus Leschik and I am convinced

that these species are synonymous. Similar interpretations have been presented by Grebe (1957 p. 60,) Bharadwaj (1962, p. 93)

Jansonius (1962, p. 62), Hart (1964, p. 1188) Freudenthal (1964, p. 226) and Visscher (1966, p. 357). Despite the wide accept ance of this view there exist widely divergent opinions concern- - 212-

ing the relative priority of the genera. A fairly comprehensive

review of the literature pertinent to this situation has been

presented by Visscher (1966 pp. 357, 358 and pp. 360-362). He

concludes that Lunatisporites must take precedence over Taeniae-

sporites. Visscher's argument is based on application of

Article 57 (* see Footnote) of the Internation Code of Botanical

Nomenclature (1966) and would appear to be unassailable.

The confusion concerning the generic concept of Lunatispo rites is illustrated by the fact that of the fifteen species assigned to the genus only five are directly comparable with

the type species. These include:-

1. Lunatisporites impervius Leschik 1955 (p . 57 , pi . 7 fig. 21)

2 . Lunatisporites detractus Leschik 1955 (p . 57, pi . 7 figs.22,23)

3 . Lunatisporites kraeuse li (Leschik) Maedler 1964 (P • 57)

4 . Lunatisporites major Maedler 1964 (p. 58, pi. 3 f ig <■ 4)

5 . Lunatisporites puntii Visscher 1966 (p . 358, pi. 14 f i gs .1-4)

I regard the first three of these species as synonyms of

Lunatisporites aoutus Leschik.

Potonie (1958) informally reinterpreted Lunatisporites, disregarding the symmetry of the taeniae and assigned to it forms which Hart (1964) recombined with Protohaploxypinus Samoilovitch emend. Hart (1964).

Footnote - Article 57 states - "When two or more taxa of the same rank are united, the oldest legitimate epithet is retained, unless a later name or epithet must be accepted under provisions of Arts.

13f, 22, 26, 58 or 59. The author who first unites taxa bearing names or epithets of the same date has the right to choose one of them, and his choice must he followed." - 213-

Potonie's interpretation was accepted and followed by Lakhanpal et at. (1960) and Potonie & Lele (1961). Although Bharadwaj

(1962) recognised the synonymy of Lunatisporites and Taeniae - sporites Leschik 1955, his formal emendation presents an inter pretation essentially similar to that of Potonie. Maedler

(1964, p. 57) presented an acceptable formal emendation, although he attempted to confine the concept to forms without a central monolete mark. A similar interpretation has been applied by

Visscher (1966).

I consider that the best balanced circumscription of the morphology of Lunatisporites is contained in the emended diag nosis of Taeniaesporites Leschik presented by Klaus (1963, p.307).

I am not sure that the proximal monolete mark described by Klaus has special significance. It's occurrence is possibly regulated by the style and relative state of preservation of the individual grain.

Forms which conform to the above concept of Lunatisporites are prominent in Upper Permian and Triassic strata of Western

Europe. They occur in Late Permian and Early Triassic deposits of the U.S.S.R. (Zauer 1965, Tschalyschev & Varyukhina 1962).

Jansonius (1962) has reported diverse assemblages from probable

Early Triassic sediments of Western Canada. The occurrence of these pollen in southern continents appears to be confined to the Early and Mid Triassic (Balme 1963, Goubin 1965 and Balme

19 70) .

Lunatisporites noviaulensis (Leschik) comb, nov.

PI. 33 figs. 1 - 10. - 214-

Selected Synonymy.

1956 Taeniaesporites noviaulensis Leschik, p. 134, pi. 23,

figs. 1, 2.

1962 Taeniaesporites novimundi (partim.) Jansonius, pi. 13,

fig. 25.

1962 Lueckisporites noviaulensis (Leschik) Grebe & Schweitzer,

pi. 11, pi. 5 figs. 7, 8.

1963 Striatites noviaulensis (Leschik) Schaarschmidt, p. 56,

pl • 15, fig. 6.

1964 Lunatisporites major Maedler, p. 58, pl. 3, fig. 4.

Description of specimens.

Pollen, bisaccate, usually with four proximal taeniae.

Outline generally diploxylonoid but ranging to haploxylonoid.

Corpus circular to elongate oval (b.c . greater than l.c.).

Cappa 1-2 microns thick, exhibiting four taeniae, although specimens with three or five taeniae are not uncommon. Shape and disposition of the taeniae is extremely variable. Taeniae appear to have been originally inflated, compression folds common occurring along the margins. Taeniae display a tendency, in some samples, towards discontinuity. Clefts between taeniae broad, varying up to 12 microns. Proximal monolete mark occas ionally discerned in the central cleft of well preserved speci mens. Cappula usually wide (about half body diameter) with relatively straight or slightly convex sides. Compression folds commonly border the cappula. Sacci large, usually well separated and distally inclined.

Dimensions.

O.L. 65 (86) 119 microns. 20 specimens measured from sample 726. - 215-

B.C. 44 (57) 70 microns.

L.C. 41 (55) 72 microns.

B.S. 27 (35) 47 microns.

L.S. 44 (55) 72 microns.

Remarks.

Although the majority of the specimens assigned to this

species clearly conform to the concept of Lunatisporites noviau

lensis as illustrated by Leschik (1956, pi. 22 figs. 1, 2), a

small but constant proportion of the various populations display

a tendency towards discontinuous taeniae or exhibit additional

taeniae. Conversely, specimens in the same samples which have

been assigned to Protohaploxypinus sp. cf. P. samoiloviohii

(Jansonius) Hart show a tendency towards development of a dis

tinct central cleft and development of four major taeniae.

Townrow (1967) reports similar variation in pollen associated with the conifer Rissikia media (Tenison-Woods) Townrow.

Lunatisporites noviaulensis has been reported from Late

Permian and Early Triassic strata throughout the world.

Comparisons.

Lunatisporites noviaulensis is more prominently diploxy-

lonoid and has broader more distinct intertaeniate clefts than

L. pelluoidus (Goubin) comb. nov. It is also invariably better

preserved. Lunatisporites sp. cf.L. puntii Visscher 1966 has an

elongate oval corpus (Z.o. greater than b.o.) and a more distinct

diploxylonoid (platysaccoid) shape. Lunatisporites transver-

sundatus (Jansonius) comb. nov. displays wrinkled taeniae and a very distinct dip 1oxy1onoid shape. - 216-

Occur renc e.

Lunatisporites noviaulensis (Leschik) comb. nov. first appears in the central portion of the Munmorah Conglomerate, the Scarborough Sandstone and the upper portion of the Caley

Formation. It ranges to the top of the Patonga Claystone to the north of Sydney but extends into the Bald Hill Claystone at Balmain Shaft. It has not been encountered regularly above this level. The prominence of L. noviaulensis often appears to be inversely proportional to the abundance of Falcisporites spp.

Lunatisporites pellucidus (Goubin) comb. nov.

PI. 32 figs. 1-5.

Selected Synonymy.

1963 Taeniaesporites sp. cf. T. noviaulensis Leschik (partim.),

Balme, pi. 6 fig. 5.

1965 Protohaploxypinus pellucidus Goubin, p. 1423, pi. 11 figs.

4-6 .

1970 Taeniaesporites pellucidus (Goubin), Balme, p. , pi. 13

f igs. 8 - 10 .

Description of specimens.

See Balme (1970, p. )

Remarks.

Balme (1970) has discussed the variation in the number and style of taeniae on forms assigned to L. pellucidus. The Sydney

Basin populationsof this species are equally diverse and conform very closely to Balme's material, even to the point of relative pres ervat ion.

Previous records.

Lunatisporites pellucidus is reported as a prominent compo- - 217- nent of the central and upper portions of the Sakamena Group of Madagascar (Goubin, 1965), where it is associated with Early and Mid Triassic microfloras. It is encountered in abundance in

the lower Scythian Mianwali Formation of the Salt Range sequence

(Balme, 1970). It is also illustrated from the Kockatea Shale

(early Scythian) of the Perth Basin, Western Australia (Balme,

1963).

Comparisons.

Lunatisporites peZZuoidus (Goubin) comb. nov. is distingu ished from L. noviauZensis (Leschik) comb. nov. by its haploxy- t lonoid shape and less distinct inter/aeniate clefts. It also has a slightly larger mean size.

Occurrence.

Lunatisporites peZZuoidus first appears in considerable abundance in the upper portion of the Caley Formation, the

Scarborough Sandstone and the central portion of the Munmorah

Conglomerate. It is most abundant in association with prominent

ProtohapZoxypinus micvocorpus (Schaarschmidt) Clarke and Strio- monosaooites morondavensis Goubin.

Lunatisporites sp. cf. L. puntii Visscher

PI. 32 figs. 6-9

1966 Lunatisporites puntii Visscher, p. 358, pi. 14 fig. 3.

Description of specimens.

Pollen, bisaccate with four proximal taeniae. Outline distinctly di ploxylonoid. Corpus spindle shaped in polar view,

Z-.a. greater than b.o. Taeniae scarcely project above proximal surface, usually difficult to detect due to preservation. Cleft - 218- between central taeniae 1-3 microns wide, but narrowing laterally.

Corpus exhibits two distal crescentic, compression folds bordering the distal area of exine detachment.

Sacci larger than corpus, often overlapping laterally. Cappula distinctly oval.

Dimens ions.

O.L. 85 (101) 121 microns. 15 specimens measured from sample 555.

B.C. 44 (50) 64 microns.

L.C. 53 (63) 86 microns.

L.S. 59 (73) 90 microns.

Remarks .

The specimens assigned here to Lunatisporites sp . cf.

L. puntii conform to the concept outlined by Visscher (1966), although they display a greater uniformity of shape and have less prominent taeniae.

Previous records.

Lunatisporites puntii is reported from the upper Bunter of eastern Holland (Visscher, 1966).

Comparisons.

Lunatisporites noviaulensis (Leschik) comb. nov. lacks the distinct diploxylonoid ("platysaccoid - Visscher, 1966) shape, and has a significantly smaller size range than forms assigned here to Lunatisporites sp. cf. L. puntii Visscher. Lunatisporites transversundatus (Jansonius) comb. nov. has a circular corpus and a considerably smaller size range. Striatites triassicus is stated by Schulz (1965) to have 5 proximal taeniae. However, it appears to have a taeniate symmetry similar to Lunatisporites. - 219-

If this organisation is established Schulz’s species would have precedence over L. punt'd.

Occurrence .

Lunatisporites sp. cf. L. puntii Visscher extends through the Tuggerah Formation, Patonga Claystone and their equivalents

It has not been encountered in sediments from the Gosford Sub group .

Lunatisporites transversundatus (Jansonius) comb. nov.

PI. 34 figs. 1-7

Selected Synonymy.

1962 Taeniaesporites transversundatus Jansonius, p. 64, pi. 14

f i gs. 3, 4.

1963 Taeniaesporites obex Balme, p. 29, pi. 6 figs. 1-3.

1966 Lunatisporites puntii (partim.) Visscher, pi. 14 fig. 1.

Description of specimen.

See Jansonius 1962, p. 64.

Dimens ions.

O.L. 67 (73) 78 microns 10 specimens measured from sample 726

B.C. 36 (39) 43 microns

L.C. 36 (38) 44 microns

B.S. 30 (33) 38 microns

L.S. 41 (45) 53 microns

Remarks .

Although the overall size range of the Sydney Basin popu lation is slightly larger they otherwise conform very closely to Lunatisporites transversundatus as described by Jansonius

(1962). The extremely thick exoexine of the cappa and compres- - 220-

sion of the originally inflated taeniae result in wrinkled,

slightly sinuous taeniae. The Sydney Basin population is indis

tinguishable from forms described as Taeniaesporites obex by

Balme (1963). Balme suggested that his species could be dis

tinguished from L. transversundatus (Jansonius) by its larger mean size and consistent thickness of the taeniae. It must be

admitted that the central taeniae of the holotype of L. trans versundatus taper laterally. However, the paratype (Jansonius,

1962, pi. 14, fig. 3) indicates that the assemblage includes

forms which cover this distinction.

Previous records.

Lunatisporvtes transversundatus (Jansonius) is a common

component of western Canadian Early Triassic microfloras (Jan

sonius, 1962). It has been reported from the Kockatea Shale of

the Perth Basin, Western Australia and the Blina Shale of the

Canning Basin (Balme, 1963). Balme also indicates its occurrence

in the Narrabeen Group of the Sydney Basin. Similar forms are also reported from the Scythian Mianwali Formation and Tredian

Formation of the Salt Range by Balme (1970).

Comparisons. This species is distinguished from Lunatisporites noviau-

lensis (Leschik) comb. nov. by its more distinct dip 1oxylonoid shape and the massive nature of the taeniae. Lunatisporites puntii Visscher 1966, as represented by the holotype, is larger and has a consistently elongate oval corpus (b.e . greater than

l.c.'). Striatopodooarpidites oancellatus (Balme & Hennelly) Hart is distinguished by the nature of the taeniae and intertaeniate clefts in specimens with four taeniae. - 221-

Occurrence .

Lunatisporites transv ersundatus first appears as a single grain in the lower portion of the Munmorah Conglomerate (sample

595). It seldom attains even moderate prominence, extending into the Bald Hill Claystone.

Genus PROTOHAPLOXYPINUS Samoilovitch Hart 1964

Type species. Protohaploxypinus latissimus Luber (in Luber &

Waltz, 1941) Samoilovitch 1953 - original

designation.

Protohaploxypinus amplus (Balme & Hennelly) Hart.

PI. 28 fig. 4.

1955 Lueokisporites amplus Balme & Hennelly, p. 93, pi. 3

figs. 24 - 28.

1958 Lunatisporites amplus (Balme & Hennelly, 1955) Potonie, p.53.

1962 Striatites amplus (Balme & Hennelly, 1955) Jizba, p. 880.

1964 Protohaploxypinus amplus (Balme & Hennelly, 1955) Hart,

p. 1179.

The list above is not intended as a synonymy, but rather as an outline of the history of the specific epithet.

Description of specimens.

See Balme & Hennelly (1955, p.93).

Rema rk s.

The concept of Protohaploxypinus amplus (Balme & Hennelly)

Hart as outlined by Balme & Hennelly (1955, p. 93) is applied here in its broadest sense. The proliferation and abundance of pollen of this general morphology in Upper Permian micro floras and the attendant nomenclatural confusion has been dis- - 222- cuss e d by Balme (I960, 1970) and Hart (1964). I have not attempted to delineate more recently defined, southern con

tinent f o rms.

Comparisons.

Protohaploxypinus amplus (Balme & Hennelly) Hart is similar

in organisation to P. sewardi (Virkki) Hart and is differentiated mainly on the basis of size and the authors intuition. It

differs from P. microcorpus (Schaarschmidt) Clarke and Proto haploxypinus reticulatus (Hennelly) comb. nov. in possessing

less numerous but well defined striae.

Occurrence.

Protohaploxypinus amplus (Balme & Hennelly) Hart was a prominent component of all Upper Permian coal measure micro floras. It is a consistent but relatively rare component of basalmost Narrabeen Group microfloras. Above this level it is extremely rare, extending into the middle part of the Narrabeen

Group.

Protohaploxypinus jacobii (Jansonius) Hart

PI. 35 figs. 1-3.

Selected Synonymy.

1946 Pityosporites spore type no. 83, Virkki, pi. 5 fig. 58

1962 Striatites jacobii Jansonius, p. 67 pi. 4 fig. 16. 17.

1964 Protohaploxypinus jacobii (Jansonius) emend. Hart, p. 1181,

text f ig. 19.

Description of specimens.

Pollen, bisaccate, striate. Amb usually slightly diploxylonoid varying to slightly haploxylonoid. Corpus oval to sub- - 223- circular. Cappa distinct, 1-2 microns thick, infrareticulate, exhibiting 8 to 12 well defined, closely spaced (less than 1 micron apart), often branching or discontinuous striae. Cappa is characteristically folded (normal to direction of striae) at the edges of the corpus, indicating that the proximal surface of the corpus was inflated significantly above the proximal sur face of the sacci. Edges of cappula usually gently convex, 18-

26 microns apart. Sacci large, distally inclined, set off proximal face of corpus.

Dimens ions.

O.L. 73 (85) 92 microns 15 specimens measured from sample 522

L.C. 47 (54) 66 microns

B.C. 48 (53) 61 microns

L.S. 41 (53) 65 microns

B.S. 25 (31) 40 microns

Remarks.

The specimens assigned here to Protohaploxypinus jaoobii

(Jansonius) Hart are identical to the specimen designated as holotype by Jansonius (1962 - Virkki, 1946, pi. 5 fig. 58).

They would appear to differ from the specimens illustrated by

Jansonius (1962, pi. 4 figs. 16, 17) which exhibit distinct equatorial saccus overlap and appear to lack the characteristic folding of the cappa. Pityosporites spore types 85 and 87 of

Virkki (1946) and Striatites sewavdi Pant do not conform to the concept outlined above.

Previous records.

This form has previously been reported from the Moolayember - 224-

Formation of south-eastern Queensland by de Jersey & Hamilton

(1967 ) .

Comparisons.

Protohap loxypinus jaoobii (Jansonius) Hart is disting uished from Protohaploxypinus sp. cf. P. samoiloviohii (Jansonius)

Hart by the folding at the edge of the cappa. It is similarly distinguished from specimens assigned to P. sewardi

(Virkki) Hart .

Occurrenc e .

Protohaploxypinus jacobii is a constant but minor com ponent of microfloras throughout the Hawkesbury Sandstone,

Wianamatta Group and their equivalents.

Protohaploxypinus sewardi (Virkki) Hart

PI. 34 figs. 8, 9, 13-15

1937 Pityosporites sewardi Virkki, p. 248, figs. 1 A - C, ZA - D

1954 Lueokisporites sewardi (Chinna-Virkki) Potonie & Klaus,

p. 534.

1955 Lueokisporites limpidus Balme & Hennelly, p. 94, pi. 3

figs. 29 - 32.

1955 Striatites sewardi (Virkki) (partim.), Pant, p. 762 , pi.19

f ig . 3

1958 Lunatisporites limpidus (Balme & Hennelly, 1955) Potonie,

p . 53 .

1962 Striatites limpidus Jansonius, p. 70, pi. 15 figs. 1, 2.

1964 Protohaploxypinus sewardi (Virkki) Hart, p. 1180, text

fig. 11 - (L. limpidus synonymised).

1970 Protohaploxypinus limpidus (Balme & Hennelly) Balme, p. ,

pi. 10 figs. 1 - 3. - 225-

The list above is obviously not a comprehensive synonymy and is intended only as an outline of the history of the specific epithets .

Descriptions of specimens.

See Balme & Hennelly 1955, p. 94, also Balme 1970, p.

Remarks.

The concept of Protohaploxypinus sewardi applied here encompasses an extremely broad morphological range. It is similar to that envisaged for nLueckisporites" limpidus by

Balme & Hennelly (1955). I have no doubt that specimens I have assigned to P. sewardi represent a polyspecial and possibly more diverse parent group. However, I have not been able to

establish any finer division of the populations.

I have extracted pollen grains identical to forms assigned to Protohaploxypinus sewardi from an undescribed species of

Arberiella Pant & Nautiyal 1960. A selection of these grains is illustrated on pi. 34.

Occurrence.

Protohaploxypinus sewardi was a dominant component of all

Late Permian coal measure microfloras examined. It is a common but rare component of basal Narrabeen Group microfloras, and is essentially absent from middle Narrabeen Group microfloras.

Protohaploxypinus microcorpus (Schaarschmidt) Clarke

PI . 30 figs.1,2.

1958 Pityosporites retioulatus {partim.) Hennelly p. 367.

1963 Striatites sp. cf. Taeniaesporites antiquus Leschik, Balme,

pi. 6 fig. 13. - 226-

1963 Striatites microoorpus Schaarschmidt, p. 55, pi. 14 figs.

6, 7.

1956b Protohaploxypinus microoorpus (Schaarschmidt) Clarke,

p. 338, pi. 41 fig. 3.

Description of specimens.

See Schaarschmidt (1963, p. 55) and Balme (1970, p. )

Remarks.

The specimens assigned here to Protohaploxypinus micro corpus (Schaarschmidt) Clarke are for the most part identical to the forms described by Schaarschmidt (1963). Minor differ ences such as the less prominent striae may possibly be related to the relative states of preservation. The Australian speci mens form a continuous morphological series with grains arbi trarily delineated and tentatively identified as Crustaesporites sp . and Striomonosaccites morondavensis Goubin.

Previous records.

This species is reported from the Upper Permian Groedner

Sandstone and Bellerophon Formation of the Dolomites (Klaus,

1963). It is a constant component of microfloras from the upper part of the Zechstein (Upper Permian) of south-western

Germany (Schaarschmidt, 1963). Clark (1956b) has identified this form in the Upper Permian Hilton Plant Series and also from a marl conformably underlying the Magnesium Limestone in

England. Clarke (p. 325) refers this section to the Lower

Permian. Balme (1970) has encountered P. microoorpus in the uppermost Permian Chhidru Formation of the Salt Range. Apart from the lower microflora described by Clarke (1956b), all - 227- these occurrences are confined to the Upper Permian and where quantitative data is available they appear to be most prominent in the uppermost Permian * - (see Footnote). Townrow (196>7) illustrates a pollen grain somewhat similar to P. microco'rpus , a number of which were attached to cuticle of Voltziopsis wolganensis.

Comparisons .

Protohaploxypinus microcorpus (Schaarschmidt) Clarke is similar to P. reticulatus (Hennelly) comb. nov., but is tenta tively distinguished by the restricted cappa development of the latter form. P. reticulatus is also smaller (on a population basis). P. microcorpus forms a continuous morphological series with forms tentatively delineated and identified as Striomono- saccites morondavensis Goubin and Crustaesporites sp. Re-exami nation of Hennelly's Appin material (particularly sample No.1918 from 1623 ft.) clearly shows that he did not distinguish between

P. microcorpus and P. reticulatus. P. microcorpus is slightly larger and has a greater number of less well defined striae than

P. amplus (Balme & Hennelly) Hart. Forms assigned to Faunipolle- nites sp. from the Late Permian Raniganj coals by Bharadwaj (1960, pi. 18 figs.232-234)are difficult to distinguish from P.micro corpus .

Footnote - There is a marked similarity of the composition of the lower (Kimberley Section) microflora described by Clarke (1956b p. 349)and those he reports from the Late Permian Hilton Plant

Series, and the well documented Zechstein occurrences of Western

Europe. This lower microflora has very little in common with the

Lower Permian (Kusel and Lebach Formation) microfloras of the - 228-

Pfalz described by Helby (1966). Kummel (1961, p. 572) suggests that the Magnesium Limestone is Upper Permian.

Occurrence.

This species is an extremely rare component of microfloras in the upper part of the Newcastle Coal Measures. It is a con stant, occasionally dominant component of lowermost Narrabeen

Group microfloras, attaining maximum prominence in the central portions of the Munmorah Conglomerate and equivalent horizons.

At this level it is associated with abundant Lunatispovites pelluoidus (Goubin, 1965). It becomes less common above the base of the Tuggerah Formation.

Protohaploxypinus vetioulatus (Hennelly) comb. nov., emend.

1958 Pityospovites vetioulatus Hennelly, p. 367, pi. 5 fig. 16,

p i . 6 figs . 17 , 18 .

1965 ? Platysacous cf. lesohiki Hart, Goubin, p. 1425, pi. 3,

f ig . 5 .

Description of specimens.

Pollen, bisaccate, striate. Outline usually slightly diploxylonoid. Outline of corpus difficult to detect, usually elongate oval ( c . I . greater than o.b.) to sub-circular. Cappa striate, elongate oval to spindle shaped, seldom extending to the edge of the grain. Cappa exine relatively thin (about 1 micron), divided into 10-15 poorly defined, closely packed

(about 0.5-1 micron apart), often branching or discontinuous, striae. Cappa is extremely sensitive to weathering processes and is seldom preserved intact. Cappula parallel sided or very slightly lensoid in shape, although the lateral extremities are - 229-

round e d . Exine of cappula thin, finely infrareticulate. Sacci

large (s.l. usually greater than c.l.), distally inclined and

encroach onto proximal surface of corpus in equatorial regions.

Darkening of the area of detachment of the exinal layers is

common. Saccus exoexine 2-3 microns thick, coarsely infra-

reticulate.

Dimens ions.

O.L. 68 (92) 130 microns - 50 specimens measured.

C.B. - not determined.

C.L. 55 (66) 83 microns

S.B. 34 (34) 56 microns

S.L. 57 (70) 95 microns

Holo typ e.

Although Hennelly designated a type locality (Appin No. 4 bore, 1623 ft. to 1697 ft. 9 in.) he did not assign a holotype.

Of the specimens illustrated, pi. 6 fig. 17 is most character

istic of the assemblage (despite the absence of the cappa) and

is here designated as lectotype - see pi. 31 fig. 1 (see also article 37, Int. Code of Bot. Nomenc.)

Remarks.

The specimens illustrated by Hennelly as "Pity osporites" retioulatus (1958, pi. 5 fig. 16, pi. 6 figs. 17, 18) are obviously poorly preserved with the cappas largely destroyed.

Although Protohaploxypinus retioulatus (Hennelly) comb. nov. et. emend, seldom displays a well preserved cappa, proximal striae are usually discernible in most populations. This feature is definitely present on a number of specimens in

Hennelly1s preparations. - 230-

Comparisons .

Protohaploxypinus reticulatus (Hennelly) comb. nov., emend.

is very similar to P. microoorpus (Schaarschmidt) Clarke and may

form a continuous morphological series with it. However, it is

smaller on a population basis, with a slightly dip 1oxy1onoid

outline and has a restricted, thinner exined cappa which seldom

extends to the equator of the grain. These characters cannot

be regarded as completely diagnostic and thus these forms are

only tentatively separated.

Occurrence.

Protohaploxypinus retioulatus is first encountered in

basalmost Narrabeen Group microfloras. It is intermittently

prominent throughout the lower two thirds of the Narrabeen Group,

becoming less common above the Patonga Claystone and its equi

valents .

Protohaploxypinus sp. cf. P. samoilovichii (Jansonius) Hart

PI. 35 figs . 4-8

1962 Striatites samoiloviohii Jansonius, p. 67, pi. 14 figs.9-11.

1964 Protohaploxypinus samoiloviohii (Jansonius) Hart, p. 1181,

text f ig. 18.

Description of specimens.

See Jansonius 1962, p. 67.

Remarks.

The specimens assigned here to Protohaploxypinus sp. cf.

P. samoilovichii encompass a broader morphological range than

the concept outlined by Jansonius (1962, p. 67) and Playford

(1965, p. 198). Some specimens exhibit a wide central cleft - 231- bet we en the two central taeniae, suggesting a similar cappa

organisation to species of Lunatisporites.

Occurrence.

Specimens assigned to this species occurred throughout the

Narrabeen Group, Hawkesbury Sandstone and Wianamatta Group. They attained considerable prominence in the central portions of the

Narrabeen Group, becoming less common above the Bald Hill Clay- s to n e .

Genus STROTERSPORITES Wilson emend. Klaus 1963.

Type species. Strotersporites communis Wilson - original

designation.

R e m a r k s .

In emending the genus Strotersporites Klaus (1963, pp.313-

316) emphasised the significance of the prominent monolete

(usually arched) mark which extends almost across the corpus between gaping taeniae. This feature alone differentiates

Strotersporites from a number of closely similar, previously validated, form genera. Hart(1964, p. 1181) regards Stroter sporites as a junior synonym of Striatopodocarpidites Sedova emend. Hart 1964, although his reasons for this are not stated.

Striatoabietites Sedova 1956 is definitely similar, that author describing a "distal" germinal furrow, which from the illus trations appears to be intimately associated with the proximal striae. In emending the genus Hart (1964, p. 1185) ignores this particular feature.

Strotersporites sp.

PI. 36 figs. 1 - 3 - 232-

Description of specimens.

Pollen, bisaccate, with multiple proximal striations and prominent monolete mark. Outline generally haploxylonoid al though a single diploxylonoid specimen was encountered. Corpus usually oval shaped (Z-. c. greater than b.c.), however, this may result from compaction as compression folds, more or less para llel to the b.o. axis, are commonly encountered on the distal surface of the corpus. Cappa distinct, 1.5 - 3 microns thick; bearing 14 - 20 striae (1.5 - 3 microns wide, 0.5 - 1 microns apart). Striae often branch and or terminate sharply. Central striae usually gape to outline a thin monolete mark which is usually arched and extends almost to edge of cappa. Exoexine of cappa infrareticulate . Cappula usually broad, more or less parallel sided, although usually bordered by compression fold.

Cappula exoexine faintly infrareticulate or unstructured. Sacci set off proximal surface with slight distal inclination. They are usually much smaller than the corpus, and are often torn off.

Dimens ions.

O.L. 90 - 95 microns 6 specimens measured from sample 726.

B.C. 48 - 63 microns

L.C. 48 - 70 microns

B.S. 35 - 44 microns

Remarks.

Although this form was only identified in a single sample it has a distinct cappa organisation which has not been reported previously from Australian microfloras. A somewhat similar form

(Striatites vichteri pi. 14 figs. 21, 22) is reported from the - 233-

Ear ly Triassic of western Canada by Jansonius (1962).

Occurrence.

Strotersporites sp. was only recognised in sample 726

(Bald Hill Claystone).

Genus STRIATOPODOCARPIDITES Zoritscheva & Sedova emend.Hart 1964

Type species. Striatopodooarpidites tojmensis Sedova - original

designation.

Remarks.

As emended by Hart (1964) Striatopodooarpidites encompasses distinctly diploxylonoid, bisaccate pollen with a prominent cappa divided into four or more striae but lacking a marked central groove. Venkatachala & Kar (1964, p. 313) traced the nomenclatural history of Striatopodooarpidites ¿ concluding that it is a junior synonym of Lunatisporites Leschik emend. Bhara- dwaj 1962. Unfortunately Bharadwaj disregarded the peculiar symmetry of the taeniae in emending Lunatisporites and presented an unacceptable interpretation of the morphology of that genus.

The generic concept of Lunatisporites is discussed in detail above and the distinctions between Lunatisporites and Striato podooarpidites can be specifically related to the symmetry of the well spaced taeniae with a prominent groove characterising the former genus.

Striatopodooarpidites oanoellatus (Balme & Hennelly) Hart.

PI. 36 f igs . 6-11

1937 Pityosporites sewardi (partim.) V i rkki, pi. 32 fig • 1 c .

1946 Pityosporites sewardi (partim.) Virkki, pi. 15 fig • 191

1955 Lueokisporite s oanoellatus Balme & Hennelly > P -• 92, pi.

figs. 11-15 - 234- 1958 Striatites oanoellatus (Balme & Hennelly), Potonie, p. 51. 1964 Striatopodocarpidites oanoellatus (Balme & Hennelly) Hart,

p. 1182 text fig. 22.

Remarks.

I regard the presence of a fringe of frilled, structured exoexine ridge surrounding the cappa as diagnostic of Striato podocarpidites oanoellatus.

Previous records. Striatopodoooarpidites oanoellatus is common in Early to

Mid Permian microfloras of Eastern Australia (Balme & Hennelly,

1955; Hill & Woods, 1964) Balme (1960, fig. 1) indicates that it extends from the Artinskian Noonkanbah Formation to the Late

Permian Liveringa Formation in Western Australia. It is recor ded in Early Permian microfloras from Tanzania (Hart, 1960) and from the Karoo of South Africa (Hart, 1963). Balme & Playford

(1967) have identified this species in the Amery Formation

(possible Mid-Late Permian) of eastern Antarctica.

C omparisons.

It is distinguished from Striatopodocarpidites pantii

(Jansonius) Balme by its more regular taeniae, and the presence of the frilled exoexine ridge surrounding the cappa.

Occurrence.

Striatopodocarpidites oanoellatus occurred in all samples between and including the Wallarah Seam and Vales Point Coal

Member in Newvale D.D.H. No. 28. It is a very rare component of basalmost Narrabeen Group microfloras. (see also range of

Striatopodocarpidites sp. cf. S. oanoellatus). - 235-

Striatopodocarpidites sp . cf. S. cancellatus (Balme & Hennelly)

PI. 36 fig. 5. Ha r t.

R e m a r k s .

These forms are very similar to Striatopodocarpidites cancellatus and are distinguished only by the absence of the frilled exoexine ridge surrounding the corpus. It is possible that these specimens could be recycled S. cancellatus from

Permian strata, the frilled ridge being removed as a result of the state of preservation.

Occurrence.

Specimens assigned to this category were first recognised in the central portions of the Hawkesbury Sandstone (Falcispo- rites Assemblage, Zonule C). They extend, as a fairly consis tent but relatively rare component of the microfloras, at least to the Razorback Sandstone of the Wianamatta Group.

Striatopodocarpidites pantii (Jansonius) Balme

PI . 36 f ig s . 13, 14.

1962 Striatites samoilovichii v a r . pantii Jansonius, p. 68,

pi . 14, f ig s . 14, 15.

? 1963 Taeniaesporites samoilovichii pantii (Jansonius) Klaus,

p. 312, pi. 14 figs. 71-73.

1965 Strotersporites pantii (Jansonius) Goubin, p. 1424, pi. 2

f i g s . 7, 8 .

1970 Striatopodocarpidites pantii (Jansonius) Balme, p. ,

pi. 12 figs. 7-9.

Description of specimens.

See Jansonius (1962, p. 68). - 236-

Remarks .

The specimens assigned to Striatopodocarpidites pantii conform very closely to the type material described and illus trated by Jansonius (1962). The development of taxonomy of this species is fully outlined by Balme (1970).

Previous records.

Striatopodocarpidites pantii was originally recorded as a common component of Western Canadian Early Triassic microfloras.

Goubin (1965) indicates that it extends through the Sakamena

Group of Madagascar (Late Permian - Late Triassic). It is reported by Balme (1970) in the Early Permian Amb Formation and the Late Permian Chliidru Formation of Pakistan. The identifi cation of this species from the Amb Formation is regarded with a degree of reserve as the cappa organisation of S. pantii displays a symmetry pattern somewhat similar to Lunatisporites and is extremely close to the cappa organisation of Protohaploxy- pinus samoilovichii (Jansonius) Hart (as I interpret this species)

These latter forms appear to be confined to Late Permian and

Triassic strata.

Occurrence.

Stviatopodocarpidites pantii occurs intermittently as an extremely rare component of microfloras in the central portion of the Narrabeen Group.

Genus STRIATOABIETITES Sedova emend. Hart 1964.

Type species. Striatoabietites brioki Sedova - original

designation.

Striatoabietites multistriatus (Balme & Hennelly) Hart.

PI. 37 figs. 18-21 - 237-

1946 ?40D Dulhunty, p. 157, pi. 7 text fig. 3.

1946 ? P 40 D de Jersey, p.7, pi. 1.

1955 Lueokisporites multistriatus Balme & Hennelly, p. 93,

pi. 2 figs. 16-20.

1964 Striatoabietites multistriatus (Balme & Hennelly) Hart,

p. 1186, text fig. 40.

1965 Striatites multistriatus (Balme & Hennelly) Tiwari, p. 192,

pi. 6 fig. 123.

Description of specimens.

Pollen, bisaccate, striate. Outline diploxylonoid in specimens with distinct sacci, more or less oval where sacci are much reduced. Corpus breadth (b . c . ) usually greater than corpus length (Z.c.) Cappa prominent, 1.5 - 2 microns thick, taeniate. Taeniae 1.5 - 2.5 microns wide, 0.5 microns apart,

0.5 - 1 microns high. Taeniae smooth, but distinctly intre- reticulate. 12 - 18 taeniae on cappa, aligned more or less parallel to the o.b. axis of the grain. Most taeniae extend across cappa, although some terminate abruptly and or bifurcate.

Cappula smooth, although some specimens (about 20% of population examined) exhibit a distal keel (5-10 microns wide) of struc tured exoexine across the corpus, normal to the long axis (b.o .) of the grain.

Nature of the sacci varies considerably. They are essen tially set off the proximal surface of the corpus more or less distally inclined and have distinct, almost straight line of exoexinal detachment on the distal surface. On some specimens the sacci are not inflated (pi. 37, figs. 20, 21). In these - 238- specimens the distal exoexine is differentiated to form saccus pads.

Dimens ions.

O.L. 50 (65) 83 microns 15 specimens measured.

C.B. 35 (48) 70 microns

C.L. 31 (42) 56 microns

S.B. up to 37 microns

S.L. up to 40 microns

Remarks.

The presence of a distal exoexinal keel on the corpus of some specimens suggests that they may be best referred Hamia- pollenites Wilson 1962 (see Jansonius 1962 , pp . 72 , 72 and Hart

1964 , pp . 1194 , 1195). Similarly the relative absence of sacci

(PI. 34 figs. 20, 21) of some specimens could be cited as reason for assigning those specimens to Aumancispovites Alpern 1958.

However, all specimens are characterised by a multitaeniate cappula and very distinct lines of distal exoexine differenti ation, which represents the saccus roots of inflated specimens.

I consider that the specimens exhibiting a distal keel and incipient saccus development as being an integral part of the morphological range of Stviatoabietites multistviatus.

Occurrence.

Stviatoabietites multistviatus is a rare component of

Permian microfloras,including those from the lower portion of the Narrabeen Group, in the Sydney Basin.

Infraturma COSTATI Jansonius 1962

Genus SCUTATIPOLLENITES nov. - 239 -

Type species. ScutatipoZZenites soutatus CBalme & Hennelly)

comb. nov.

Selected Synonymy.

1956a MarsupipoZZenites { partim.) Balme & Hennelly, p. 60.

1962 Vittatina {partim.) Bharadwaj p. 100.

1965 Pakhapites {partim.) Hart, p. 104.

Diagnosis.

Pollen, incipiently bisaccate. Outline oval in polar view, oval to almost semi-circular in lateral view. Structured cappa incompletely developed, comprised of discrete elements which have a surface expression similar to microverrucae. These elements display distinct alignment, simulating taeniae. Sacci are very small, distally inclined and confined to the extreme lateral and distal surfaces.

Comparisons.

The structure of the exoexine of ScutatipoZZenites is essentially similar to that of MarsupipoZZenites Balme & Hennelly

1956. However this genus differs from MarsupipoZZenites in lacking a proximal tetrad mark; in its more distinctly oval shape {o.b. greater than o.Z.) and its possession of distinct sacci in all specimens. It differs from Aumanoisporites Alpern

1958 in having an incompletely developed cappa and taeniae sy s t em.

Remarks.

The similarity of the proximal exoexine of forms assigned here to SoutatipoZZenites gen. nov. and MarsupipoZZenites Balme

& Hennelly 1956 obviously excludes them from Aumanoisporites - 240-

Alp ern 1958. Hart (1965, p. 104) proposed a genus Pakhapites to accommodate Praecolpati without aperture but with proximal striations", assigning to it forms referred here to

Seutatipollenites. I believe that Pakhapites is indistingu ishable from Vittatina as diagnosed by Hart (1965, p. 50 "...

This genus differs from other Striatiti by it's absence of sacci. ..."). Vittatina Luber ex Wilson 1962 is almost certainly a junior synonym of Aumaneisporites Alpern 1958 (see p.242 ).

SeutatipoUenxtes seutatus (Balme & Hennelly) comb. nov.

PI. 37 figs. 12 - 16.

Selected Synonymy.

1956a Mavsupipollenites seutatus Balme & Hennelly, p. 62, pi. 2

f igs . 38 - 41.

1962 Vittatina seutata (Balme & Hennelly), Bharadwaj, p. 100.

1965 Pakhapites seutatus (Balme & Hennelly), Hart, p. 105,

text fig. 254.

Description of specimens.

Pollen, incipiently bisaccate. Outline oval in polar view, oval to semi-circular in lateral view. Proximal and lateral exoexine structured, forming an incompletely developed cappa.

The cappa is comprised of discrete columellate elements which have a surface expression similar to grana and flattened microverrucae. These elements display a distinct alignment, simulat ing taeniae. This development is confined to the central proximal surface and gives way to randomly scattered elements approaching equatorial regions. Structured exoexine extends onto the extreme limits of the distal surface, where it rapidly grades into the smooth, apparently unstructured exoexine of the - 241- cappula. Intexine smooth, about 0.5 microns thick. Sacci development is confined to the extreme lateral or distal sur faces. Sacci are invariably distally inclined, often projecting above the general distal surface as small, apparently deflated folds of exoexine. Specimens tend to fold along axes more or less parallel to the l.c. axis.

Dimensions.

O.L. 25 (38) 46 microns 10 specimens measured.

B.C. 25 (34) 42 microns

L.C. 21 (27) 40 microns

D.C. 21 (35 microns.

Holo type .

Balme & Hennelly 1956b, pi. 2 fig. 39 - designated as lectotype by Bharadwaj (1962, p. 100).

Comparisons.

Scutat'ipo'iZen'ites soutatus is differentiated from Auman- oisporites fasoiolatus (Balme & Hennelly) comb. nov. by the well developed cappa of the latter form. It is distinguished from striate specimens of Marsupipollenites triradiatus Balme

& Hennelly in lacking a proximal tetrad mark, having distinct sacci development and a more or less unidirectional alignment of the proximal exoexine elements.

Remarks.

Balme & Hennelly (1956b) report Soutatipollenites soutatus only from the Early Permian Greta Coal Measures.

Occurrenc e.

This form occurs as a rare but constant component of - 242-

microfloras between and including the Wallarah seam and the

Vales Point Coal Member in Newvale D.D.H. No. 28. It also

occurs as a rare component of basalmost Narrabeen Group micro

floras in southern and western areas of the Sydney Basin.

Genus AUMANCISPORITES Alpern 1958.

Type species. Aumanoisporites striatus Alpern - original

designation.

Selected Synonymy.

1953 Vittatina Luber- Samoilovitch, p. 44.

1956a Marsupipollenites (partirti.) Balme & Hennelly, p. 60.

1958 Aumanoisporites Alpern, p. 84.

1960 Protosaooulina Malyavkhina (partim.) Hart, p. 8.

1962 Vittatina Luber ex Wilson, p. 24. (February, 1962).

1962 Vittatina Luber ex Jansonius, p. 73, (April, 1962)

1962 Aumanoisporites Alpern emend. Jansonius, p. 76.

1965 Pakhapites Hart, p. 104.

1966 Costapollenites Tschudy & Kosanke, p. 62.

Remarks.

Despite the arguments presented by Clarke (1965b, p. 340) and Helby (1966, p. 685) there can be little doubt that Auman oisporites Alpern 1958 has priority over Vittatina Luber ex

Wilson 1962. Prior to Wilson’s designation of Vittatina subsaooata Samoilovitch as type species (Wilson 1962, p. 24) Vitta tina was not a valid taxon. The most acceptable interpretation of the genus is that of Hart (see Vittatina3 Hart 1964, p. 1195).

It is considerably broader and embraces the entire morphological range which Wilson (1962) ascribed to Vittatina and Jansonius - 243-

(1962, pp. 73-76) referred to Vittatina and Aumaneisporites.

Hart (1965b, p. 104) proposed a new genus Pakhapites to

accommodate "praecolpati without aperture but with proximal

striations." Hart does not give a comparative diagnosis and

it would appear that forms assigned to Pakhapites are adequately

circumscribed by his diagnosis of Vittatina Luber ex Jansonius

1962 (same volume, p. 50) - "Striatiti with or without sacci."

Aumaneisporites faseiolatus (Balme & Hennelly) comb. nov.

PI. 37 fig. 17

1952 ?P23C Balme, p. 9, fig. 45 (not 44).

1956a Marsupipollenites faseiolatus Balme & Hennelly, p. 62,

pi. 3 fig. 42-45.

1962 Vittatina faseiolata (Balme & Hennelly) Bharadwaj, p. 100.

1965 Pakhapites faseiolatus (Balme & Hennelly) Hart, p. 105,

text fig. 252.

Description of specimens.

Pollen, bisaccate - usually very poorly developed sacci,

cappa taeniate. Outline oval in polar view, more or less oval

in lateral view. Cappa well developed, exoexine divided into

taeniae which run sub-parallel to the b.c. axis of the grain.

Taeniae randomly bifurcate or terminate abruptly. 10-15 taeniae present on the cappa, 2-3 microns wide, 0.5-1 microns high, o . 5 -

1 micron apart. Exoexine of distal surface not noticeably struc

tured, smooth. Exoexine thin. Sacci usually poorly developed,

confined to the lateral edge of the distal surface, distally

inclined. In specimens in which sacci are not apparent, there

is a recognisable differentiation of the lateral distal exoexine - 244- There is a tendency for specimens to fold along axes parallel

to the l. o . axis of the grain.

Dimens ions.

B.C. 32 (40) 53 6 specimens measured.

L.C. 29 (37) 47

Holo type.

Bharadwaj (1962, p. 100) has designated the syntype illus

trated by Balme & Hennelly (1956a, fig. 42 on plate 3) as lecto-

type.

Comparisons.

Aumancisporites fasoiolatus (Balme & Hennelly) comb. nov.

is differentiated from Soutitopollenites soutatus Balme &

Hennelly) comb. nov. by the fully developed nature of its cappa.

The taeniae of A. fasoiolatus have a greater tendency to bi

furcate and or terminate abruptly than those of A. striatus

Alpern populations I have examined. The mean size is also

considerably less. Aumancisporites subsaooata (Samoilovitch)

comb. nov. (S amo i lo vitch 1953 , p. 44, pi. 9 figs. 4a, b) is

larger, and has a greater number of taeniae.

Occurrence.

A. fasoiolatus occurs as a very rare component of micro

floras below, including and immediately above the Vales Point

Coal Member in Newvale D.D.H. No. 28.

Genus MARSUPIPOLLENITES Balme & Hennelly 1956. emend. Balme, 1970.

Type species. Maruspipollenites triradiatus Balme & Hennelly

emend. - original designation.

Remarks.

Balme (1970, p. ) has reinterpreted and emended the genus - 245-

Marsupipollenites to include forms characterised by a proximal tetrad mark on a sculptured exine, bearing a distal sulous which may or may not be bordered by folds. Three of the species ori ginally assigned to Marsupipollenites (M. fasoiolatus B. & H.

, M. soutatus B. & H. and M. sinuosus B. & H. ) have previously been referred to other genera (Bharadwaj, 1962;

Hart, 1965) .

Marsupipollenites is differentiated from Scutatipollenites gen. nov. by the absence of the proximal tetrad mark and more distinct but still incipient sacci development in the latter form.

It differs from Valesipollenites gen. nov. by its incompletely developed cappa and lacks the relatively well developed sacci of that genus.

Marsupipollenites triradiatus Balme & Hennelly emend.

PI. 37 figs. 1-11.

Selected Synonymy.

1945 P8A partim. Dulhunty

1946 P8A partim. de Jersey

1952 P8A Balme

1952 P 9 C Balme

1956a Marsupipollenites triradiatus Balme & Hennelly, p. 60,

pi. 2, figs. 29-35 .

1956a Marsupipollenites triradiatus forma striatus Balme &

Hennelly, p. 61, pi. 2 figs. 36, 37.

1965 Marsupipollenites striatus (Balme & Hennelly) Hart, p. 104,

text fig. 250. - 246-

Description of specimens.

Pollen with proximal trilete mark, occasional incipient sacci development. Outline more or less oval, breath (c.b. ) usually greater than (o.t. ) of grain in unfolded specimens. The majority of specimens are usually folded,once or twice along axes more or less parallel to the o.1. axis. Exine two-layered, intexine thin, usually indistinct. Exoexine is usually deline ated into two distinct areas. One area,0.5-2 microns thick is structured, comprised of closely spaced, columellate elements with a surface expression similar to small, irregular, flattened verrucae. This area covers the proximal and equatorial regions of the grain, extending slightly onto the distal surface. At the proximal pole a distinct trilete mark occurs. Laesurae vary in length up to 12 microns, one laesura which is more or less parallel to the short axis (c.Z.) of unfolded grains, or alter natively, normal to this axis in folded grains, is shorter than the other two. The structural elements of this part of the exine, particularly in the vicinity of the proximal pole often show a tendency to a rough, sub-parallel alignment, simulating taeniae.

The second smaller exoexinal area is confined to the distal surface and is oval in shape, the outline being more or less parallel to the shape of the grain. The exoexine in the area is not obviously structured, is smooth and o.5-l micron thick.

It grades sharply into the structured, exoexinal area. In some specimens, the exoexine is differentiated into very small, inci pient sacci development at the lateral (along c.b. axis and normal to it) junction of the exoexinal areas. - 247-

Dimensions .

B.C. 40 (56) 68 microns

L.C. 41 (51) 64 microns - 25 unfolded specimens measured from

samp1e 981.

Remarks.

Marsupipollenites triradiatus is predominantly encountered in the folded form with two folds on the distal surface,which exhibit structured exoexine. Balme (1970, p. ) interprets the folds and area between as a sulcus. I consider the so- called sulcus as only part of an area, possibly analgous to the cappula of bisaccate pollen, which in these grains is mostly concealed under the folds. The constant nature of the folding is obviously due to compression of the original inflated grain.

I interpret the original grain as having a strongly convex proximal surface sloping away from a flatter proximal pole in lateral view. The distal surface was probably concave. Pollen resembling Marsupipollenites triradiatus have been extracted from Polytheca elongata, a sporangium of uncertain affinities, by Pant & Nautiyal (1960).

Occurrence.

Marsupipollenites triradiatus is a common component of microfloras in samples between and including the Wallarah Seam and the Vales Point Coal Member in Newvale D.D.H. No. 28. It occurs less commonly in samples immediately above the Vales Point

Coal Member and samples from the basalmost Narrabeen Group in the south and west of the Sydney Basin. It gradually disappears in younger lower Narrabeen Group microfloras. - 248-

Inf raturma DISACCITRILETI Leschik 1956.

Genus VALESIPOLLENITES nov.

Type species. ValesipolZenites evansi gen. et sp. nov. -

here- designated.

Diagnosis.

Pollen, bisaccate. Outline oval in polar view, almost oval to bean shaped in lateral view. Cappa thick, exhibiting distinct tetrad mark in the vicinity of the proximal pole. Sacci relatively small, restricted to equatorial and distal surfaces, distally inclined.

Comparisons.

Valesipollenites gen. nov. differs from Jugasporites

Leschik 1956 and Tri adispora Klaus 1964 in having a thick, distinct cappa, constantly elongate corpus and characteristi cally restricted sacci. It differs from Parcisporites Leschik

1955 in possessing a proximal tetrad mark. If differs similarly from Parvisaccites Couper 1958 (possibly a junior synonym of

Parcispovites .) It is very similar to Klausipollenites Janso- nius 1962 (especially the interpretation of Klaus, 1963) but is differentiated by the tetrad mark. Marsupipoiienites (Balme &

Hennelly) emend, is similar, but differentiated by absence of a distinct cappula and obvious intrareticulation.

Valesipollenites evansi sp. nov.

PI. 38 f igs . 6-20

Description of specimens.

Pollen, bisaccate, generally diploxylonoid. Outline more or less oval in polar view, hemispherical to bean-shaped in - 249-

lateral view. Corpus oval in polar view, oval to almost bean

shaped in lateral view, (corpus breadth usually greater than

corpus length.) Cappa 1.5 - 2.5 microns thick, very distinct

but finely intrareticulate, thickening away from the proximal

pole. Clear tetrad mark visible in vicinity of proximal pole,

laesurae up to 10 microns long, one laesura (parallel to short

axis of corpus) usually shorter than others. Cappula distinct,

thin, leptomate, often torn. Cappula intrareticulation becomes

extremely fine approaching the leptoma, where it is smooth.

Detached intexine apparent in rare specimens, about 1 micron

thick. Sacci limited to extreme equatorial and distal surfaces, not detached from intexine in many specimens, but joined by

long columellae.

Dimensions. - see key.

0 . L . 36 (49) 60 microns. 50 specimens measured from sample 981

C . B . 30 (41) 50 microns

C . L . 30 -- 45

C . D . 32 __ 42

Type locality.

Vales Point Coal Member, Newvale D.D.H. No. 28.

Holotype.

Slide 981/4 31.0 115.0 PI. 38 figs. 19. 20 (size 57

microns)

Comparisons.

Valesisporites evansi sp. nov is smaller and is further distinguished from Klausipollenite s sp . by the presence of the

tetrad mark. Klausipollenites sohaubergeri (Potonie & Klaus) - 250-

Jansonius has a larger mean size and lacks a tetrad mark.

Illinites parvus Klaus and Jugasporites schaubergeroides Klaus exhibit very distinct thinning of the cappa in the vicinity of the trilete mark and sacci which are joined equatorially.

Occurrence.

This species is a minor but common component of microfloras between and including the Wallarah Seam and the Vales Point

Coal Member in Newvale D.D.H. No. 28. It is a rare component of microfloras immediately above the Vales Point Coal Member.

Non Striate pollen.

Corystospermaceous pollen are very prominent components of southern continent Triassic microfloras. They are characterised by a distal colpus (anacolpate in the sense of Erdtman and Straka,

1961). Pollen of this type have been extracted from Pteruchus africanus Thomas ,P. dubius Thomas, P. simmondsi (Shirley) Thomas,

P. petasatus Townrow, from an unnamed pollen organ associated with IHoegia papillata Townrow and from isolated sporangia

(similar to Arberiella Pant & Nautiyal 1960) which are probably associated with plant remains tentatively identified as ?Thinnfe-

Idia oallipteroides Carpentier. Townrow (1962, p. 40) indicates that pollen extracted from Thuringia Remy 1953, Mas culostrobus

Seward 1911 and Arberiella Pant & Nautiyal 1960 are also colpate, although pollen of Thuringia oallipteroides Remy (see Helby, 1966 , p. 680) and other pollen extracted from some Arberiella like sporangia (see Remarks - Protohaploxypinus limpidus p. 225) dis play obvious proximal differentiation.

Townrow delineates the colpate forms listed above from the leptomate pollen produced by Harrisiotheoum Lundblad 1961, - 251-

PcT'me'Lreuthia Krasser 1948 Caytonanthus Harris 19 37 , Ullmania

Goeppert and Ruhleostaohys Roselt 1956. He goes on to state

(p. 40) ..."There is only one character which divides the material

(pollen from the above fructifications) into two clear cut groups,

and that is the nature of the germination area, whether a colpus

or a leptoma. The two groups are unnatural, however." I agree

that the colpus and leptoma are important diagnostic characters.

However, as a result of differential preservation the colpate

nature of a pollen grain is often not detectable and a leptoma

may be interpreted.

The unfortunate choice of holotype and the inadequate diag

nosis of Alisporites opii Daugherty have been major contribu

tions to the nomenclatural confusion which surrounds pollen

genera of this general morphology. Helby (1967 a, p. 68) indi

cated that the holotype of A. opii was not characteristic of the

population in the Chinle Formation, suggesting that the genus

be retained pending investigation of the type material. Balme

(1970, p. ) also suggests that the holotype is atypical of the

Chinle material, and in reference to the distal morphology of

the specimen concludes "... this could represent a random rent in

an undifferentiated cappula rather than a sulcus." Re-examination

of the type preparation is obviously warranted.

Having examined Chinle Formation material (kindly supplied

by Dr. J. Jansonius) I believe that Alisporites opii population

is neither colpate nor distinctly leptomate (see pi. 41 figs. 24,

25) .

Other genera to which pollen exhibiting a distal colpus or - 252- leptoma have been assigned most commonly include Falcisporites

Leschik 1956, Pityosporites Seward 1914, Pteruchipollenites

Couper 1958 and Sulcatisporites Leschik 1955. Of these Pityo- sporites is the most controversial, having been raised on the basis of a transverse section of a single grain. Thus any inference to the three dimensional external morphology of this genus is, at best, speculative. Clarke (1965a, p. 308) suggests that Pity osporites should be abandoned as a confused taxon

(Article 65 - Int. Code Bot. Nomenc.) This suggestion has con siderable merit.

Falcisporites Leschik 1956 has been emended by Klaus (1963, p. 332) to include forms exhibiting a "sulcus" extending across the distal surface of the corpus. Although the illustration of the holotype of Falcisporites zapfei (Potonie & Kremp 1954, pi. 10 fig. 9) is difficult to interpret (I consider it to be leptomate), the excellent photographs of Klaus (1963, pi. 18, figs. 85-87) leave no doubt that the "sulcus" is leptomate in nature. Balme (1970) applies a slightly broader interpretation of Klaus' diagnosis including both colpate (F. stabilis Balme

1970) and leptomate (F. nuthallensis Balme 1970) forms. In view of the difficulty in distinguishing colpate from leptomate forms in other than well preserved material I regard this as a most practical approach.

Pteruchipollenites Couper 1958 has previously been regarded as a junior synonym of Alisporites. However, in view of the above discussion concerning the validity of Alisporites. This may no longer apply. Balme (1970) suggests that Pteruchipolle- - 253- nites is a junior synonym of Faleisporitess although this implies a broad interpretation of the latter genus. I have examined the type material of Pteruehipollenites and I am con vinced that it is colpate. Valid arguments could be produced for the retention of Pteruehipollenites to distinguish colpate forms. However, I do not believe that I could delineate satis factorily all Faleisporites (leptomate forms) from Pteruchi-

\pollenites (colpate forms) occurring in my material.

I have examined the type material of Suleatisporites Leschik

1955. The holotype of S. interpositus displays a distinct colpus, which appears to be lipped, however I suspect that this speci men is an end member of a broad morphological pollen suite, the major part of which Leschik described as Pity osporites devolvens

Leschik.

The holotype of S. splendens Leschik has been rephotographed by Grebe & Schweitzer (1962, pi. 9 fig. 2), these authors sug gesting that the species is a junior synonym of "Pityosporites” zapfei Potonie & Klaus 1954.

Infraturma DISACCIATRILETI Leschik 1956.

Genus FALCISPORITES Leschik emend. Klaus 1963.

Type species. Faleisporites zapfei (Potonie & Klaus) Leschik -

original designation.

Remarks.

The non-striate, bisaccate pollen comprise the dominant component of Australian uppermost Permian and Triassic micro floras. As mentioned previously a large proportion of these forms are probably of corystospermaceous origin. The first formal - 254- descriptions are those of Hennelly (1958) in which he assigns two species to Pity osporites Seward 1914 (P. nigraoristatus

Hennelly and P. retioulatus Hennelly). Although the holotype of P. tligracristatus is not obviously colpate, other specimens in the poorly preserved type population display a distinct colpus. Specimens from similar but better preserved basal

Narrabeen Group microfloras are usually colpate. I believe that P. retioulatus is striate.

De Jersey (1964) discusses this type of pollen, delineating four species in the Ipswich material, referring three colpate species (including Alisporites australis de Jersey) to fructi fications of Pteruchus Thomas 1933. The fourth species CAli- sporites parvus de Jersey) appeared to be leptomate and was assigned to the Coniferophyta . From the preamble above it is evident that at least six pollen organs contribute colpate bisaccate pollen of this general morphology to the dispersed micro floras. It is also reasonable to assume that a number of other plants contribute leptomate pollen.

I am not convinced that marginal size variation and the various body!saccus ratios are sufficiently understood to be used as diagnostic characters. As the presence of a detectable colpus is also largely dependant on the relative state of pre servation of the individual grain I consider that I would not be justified in delineating individual species at this stage.

Faloisporites nigraoristatus (Hennelly) comb. nov.

PI. 39 figs. 1-6.

Selected Synonymy.

1953 Type 38B Taylor (a), pi. 16. - 255-

1953 Type 38B, C, E, F, G. Taylor (b), p. 162, 163.

1958 Pityosporites nigraoristatus Hennelly, p . 366, pi.

figs . 13-15 .

1962 Alisporites australis de Jersey, p. 8, pi . 2, fig.

pi. 3, figs . 3, 4.

1962 Alisporites parvus de Jersey, p . 9 , pi. 4 , figs. 1-

Remarks.

I am not confident that the forms indicated in the synonymy above can be delineated satisfactorily. De Jersey (1962,)

distinguishes A lispori tes parvus from A. australis (p . 9). He

indicates that the colpus is probably only observed in...."well preserved, suitably orientated specimens". I would also include

in a comprehensive synonymy species assigned by Jain (1968) to ,0941) Alisporites Daugherty/, Jansoniuspollenites Jain 1968 and Pteru- chipollenites Couper 1958.

Occurrence.

Faloisporites nigracristatus is encountered as a very rare component of Sydney Basin Permian coal measure microfloras. It is particularly abundant throughout the overlying Late Permian -

Triassic section, although noticeably less prominent when it is associated with Lunatisporites spp. and Protohaploxypinus sp. cf

P. samoilovichii (Jansonius) Hart.

Genus KLAUSIPOLLENITES Jansonius 1962

Type species. Klausipollenites schaubergeri (Potonie & Klaus)

Jansonius - original designation

Remarks.

Jansonius (1962, pp. 55, 56) proposed Klausipollenites to - 256- accommodate forms in which sacci are generally confined to the equatorial and distal surfaces of the corpus and which may or may not exhibit equatorial continuation of the sacci. Although

K. sohaubergeri was chosen as the type species Jansonius used a relatively broad interpretation of the genus. Klaus (1963, pp.

333-34) adopts a more restricted interpretation, but emphasises the lateral elongation of the corpus.

Klausipollenites sp.

PI. 38 figs. 21-23.

Description of specimens.

Pollen, bisaccate, generally diploxylonoid. Outline oval in polar view, sub-hemispherical to crescent shaped in lateral views. Corpus oval in polar view, oval to kidney shaped in lateral view (corpus breadth is always greater than corpus len gth) . Cappa quite distinct, 2-3 microns thick, intrareticulate, thickening away from the proximal pole. Detached intexine 0.5-

1 micron thick. Cappula relatively thin, very finely intrareticulate to smooth, possibly with a leptoma which is prone to rupture. Sacci restricted to extreme lateral and distal surfaces, distally inclined. Exact limits of sacci difficult to ascertain due to similarity of intrareticulation of cappula, although there is a slight tendency towards elongation of the brochi on the sacci. In marginal regions the exoexine of the sacci is joined to the intexine by long columellae. Sacci are not equatorially continuous.

Dimensions.

O.L. 63 (67) 75 - 20 specimens measured.

C.L. 48 (54) 62 - 257-

C.B. 45 (48) 34

C.D. 37 (40) 45

Comparisons.

Klaus ip o ZZ enirtes sp . is delineated from the type species by the shape of the corpus and restriction of the sacci. It is marginally larger, has a different corpus shape and more obvious ly restricted sacci than the Canadian species assigned to KZaus'Z-

\poZZenites by Jansonius (1962 , pp. 56-58). It is morphologically similar to VaZesipoZZenites evansi sp. nov. but is larger and lacks a tetrad mark.

Remarks.

This species conforms well to Klaus’ (1963) interpretation of KlausipoZZenites ^ although equatorial sacci extensions or thickened equatorial exoexine ridges were not observed. Balme

(pers. comm.) reports that forms similar to KZausi-p oZZ enite s sp . are relatively abundant in parts of the Liveringa Formation of the Canning Basin.

Occurrence.

KlausipoZZenites sp. occurs as a rare but constant compo nent of Newcastle Coal Measure microfloras. In the basal Narra- been Group microfloras above the Vales Point Coal Member it becomes extremely rare.

Genus VESICASPORA Schemel 1951

Type species. Vesicaspora wilsonii Schemel - original desig

nation.

Remarks.

Schemel (1951, pp . 748-749) was quite explicit in defining - 258-

V esioaspora to include bisaccate to sub-bisaccate pollen in which the long axis of the corpus (in polar view) was normal to the axis of the sacci. The cappula of these forms was illus trated as being extremely narrow. The general morphology of the genus was adequately illustrated by Wilson and Venkatachala

(1963), resulting from a study of a topotype population. However, the reinterpretation of the genus by these authors suggested that the corpus (intexine) was circular in outline in both polar and lateral views. This is obviously contrary to the morphology displayed by most of the specimens they illustrated. Although many of the specimens illustrated show obvious lateral continu ation of sacci (or saccus) the illustration (text fig. 1) given by these authors is a rather extravagant exaggeration of this feature. Klaus (1963), regarded the genus as being character ised by a corpus which is constantly broader than long. He cited this feature as being a contradistinction to Klausipollen- ites Jansonius 1962. This has been particularly constant character of all Vesioaspora populations I have examined.

Balme (1970) accepted the reinterpretation of Vesioaspora proposed by Wilson & Venkatachala (1963) and on this basis assigned forms of the general morphology to Sulcatisporites

Leschik emend. Nilsson 1958. Balme1s interpretation of Sutoa- tisporites was essentially similar to the still valid concept of Vesioaspora as described by Schemel and subsequently illus trated by Wilson and Venkatachala. However, anticipating future interpretation problems concerning Sulcatisporites Balme indi cated that Votziapites Malyavkhina 1964 may be an alternate form - 259- genus for this type of pollen.

Vesicaspora ovata (Balme & Hennelly) Hart

PI. 38 figs. 1-5.

Selected Synonymy.

1955 Florinites ovatus Balme & Hennelly, p. 96, pi. 5 figs.49-52.

1960 Vesicaspora ovata (Balme & Hennelly) Hart, p. 10, pi. 3

fig. 33.

1960 Pityosporites ovatus (Balme & Hennelly) Lakhanpal, Sah &

& Dube, p. 115, pl.l fig. 17.

1962 Sulcatisporites ovata (Balme & Hennelly) Bharadwaj, p. 97. non 1962 Alisporites ovatus auct. non. (Balme & Hennelly)

Jansonius, p. 58, pi. 13, figs. 1, 2. non 1963 Alisporites ovatus auct, non. (Balme & Hennelly)

Schaarschmidt p. 59, pi. 15, figs. 18, 19, pi.16 fig.

1-5 .

Description of specimens.

See Balme (1970, p. ).

Dimens ions.

O.L. 29 (37.5) 47 microns. 50 specimens measured from sample 981.

B.C. 21 (25) 30 microns.

L.C. 24 (33) 43 microns.

The forms measured in the study represent a distinct size group within the Vesicaspora ovata population. A second, slight ly larger (20-40%) group occurred less commonly in the same material and was morphologically indistinguishable apart from the size variation.

Remarks.

The organisation of the Vesicaspora ovata forms encountered - 260- in the present study was predominantly bisaccate in tendency.

Only a few specimens showed distinct equatorial detachment of the exoexine. A structure analogous to the "lateral fold" on the proximal surface of the corpus of Vesicasp ora wilsonii

Schemel (Wilson and Venkatachala, 1963, pi. 1 figs. 7-9, 13,

14 and Helby 1966 p. 677) was not encountered.

Occurrence.

V esioaspora ovata occurred in all samples below and in cluding the Vales Point Coal Member in Newvale D.D.H. No. 28.

It is noted that it is more abundant in coaly material. It occurs intermittently in basal Narrabeen Group microfloras.

Genus VOLTZIAPITES Malyavkhina 1964.

Type species. Voltziapites vulgaris (Malyavkhina) emend.

Malyavkhina - original designation.

Diagnosis. (translated from Malyavkhina, 1964, p. 137).

"Large oval pollen with two large, indistinct, sacci surrounding the body; body large and oval exhibiting a narrow or broad, usually spindle shaped, area of thinner exine."

R e m a r k s .

I interpret the principal features of Voltziapites as comprising the distinctly oval shape (? hap 1oxylonoid) , rather indistinct corpus - saccus delineation in proximal and equa torial regions and a narrow, often fusiform cappula. It is obvious that this concept is closely similar to Bharadwaj's interpretation of the morphology of Sulcatisporites Leschik

1955 (Bharadwaj, 1962). There exists generally confused agree ment (Potonie, 1958; Balme, 1970; Helby above) that the holotype - 261- of Suloatisporites interposus Leschik is indistinguishable from a number of previously validated species. Balme (1970) has recognised the similarity of the concepts of Suloatisporites and Voltziapites3 and suggested Voltziapites as a possible alternative to Suloatisporite s in view of the considerable doubts concerning its validity.

In discussing Voltziapites Malyavkhina indicates that species assigned to the genus display a low range of variability, most of this being directly attributed to preservation and style of compression of the individual grains. She states that the type species, V. vulgaris (Malyavkhina) Malyavkhina is indis tinguishable from the specimen illustrated as "Sporemorph C" by Lundblad (1949). Voltziapites is distinguished from Obla- tinella Malyavkhina 1956 by its constantly oval outline and from Lebachiaoites Malyavkhina 1964 by the well defined sacci of the latter genus.

Voltziapites Malyavkhina 1964 is superficially similar to Vesioaspora Schemel 1951. Vesioaspora is characterised by an oval corpus (l.c . greater than b.o.) which is usually distinct and a tendency towards lateral exine detachment (monosaccate development).

Some specimens assigned to Vesioaspora ovata (Balme &

Hennelly) Hart could be suitably accommodated by the genus

VoItziapites.

Voltziapites balmei sp. nov.

PI. 39 figs. 7, 8.

1955 Florinites eremus (partim.) Balme & Hennelly, pi. 5 figs.

46, 47. - 262-

71964 Suloatisporites sp. B, Bharadwaj & Salujha, p. 212, pi. 12

fig. 161.

71965 Vesicaspora sp., Salujha, p. 232, pi. 2 fig. 36.

1966 Suloatisporites Bharadwaj & Tiwari, pi. 2 fig. 16.

71967 Suloatisporites sp. Maheshwari, p. 277, pi. 8 fig. 68.

Description of specimens.

Pollen, bisaccate. Outline predominantly haploxylonoid

(usually distinctly oval in polar view), more or less oval in

lateral view. Cappa oval in shape (long axis of cappa parallel

to l.o .), 1-1.5 microns thick, very finely infrareticulate.

Corpus oval to circular, outline extremely difficult to detect beyond the cappa. Cappula characteristically narrow, more or

less parallel sided, seldom more than 5 microns wide. Sacci

large, display only slightest distal inclination. Lateral

exinal detachment occasionally isolates the corpus. Saccus exoexine characteristically thin, coarsely infrareticulate .

Dimens ions.

O.L. 78 (94) 113 microns. 20 specimens measured from sample 981.

L.C. 57 (66) 74 microns

Type locality.

Newvale D.D.H. No. 28 at 300 ft. (Vales Point Coal Member).

Holo type .

Slide 981/3 25.0 114.0 Illustration - PI. 39 fig. 7.

Remarks.

The illustrations of Florinites eremus presented by Balme

& Hennelly (1955, pi. 4 figs. 45 - 48) included two distinct species. The concept of the species as outlined by these authors - 263- would apply only to the specimens illustrated by figures 45 and 48. The specimens illustrated on figures 46 and 47 show features which I interpret as the distal saccus roots of an essentially bisaccate grain.

Comparisons .

Vesioaspora ovata (Balme & Hennelly) Hart encompasses morphographic miniatures of Voltziapites balmei sp. nov. Volt ziapites vulgaris (Malyavkhina) Malyavkhina has a distinctly oval corpus (b.o. greater than l.o.) and a large almost cir cular cappa.

Previous records.

Balme & Hennelly indicate that Florinites eremus is a particularly common component of Western Australia Mid to Late

Permian coal measure microfloras and also occurs in equivalent microfloras in New South Wales. It is not possible to interpret which part of their population they are discussing. Similar forms have been described from the Raniganj Coal Measures (Bhara- dwaj & Salujha, 1964; Salujha, 1965 and Maheshwari, 1967) and the Karanpura Coal Measures (Bharadwaj & Tiwari, 1966) of India.

Occurrence .

Voltziapites balmei sp. nov. was recovered only from samples taken from the Vales Point Coal Member.

Genus VITREISPORITES Leschik emend. Jansonius 1962.

Type species. Vitreisporites pallidus (Reissinger) Nilsson

Leschik (1955, p. 53) assigned V. signatus as type species of Vitreisporites. However, Balme (1970 p. ) suggested that

V. signatus is a junior synonym of V. pallidus. I agree with

Balme. - 264-

Remarks .

The diagnosis of Vitveisporites given by Leschik describes a weak trilete mark on the cappa. I have examined the type material and although I could see the feature on the holotype referred to by Leschik, it was not present on several other specimens I located. I am not convinced that feature was a trilete mark.

Vitveisporites pallidus (Reissinger) Nilsson 1958 .

PI. 40 f igs. 3-5 .

Selected Synonymy.

1940 Pityospovites pallidus (nom. nud.) Reissinger, p. 14 .

1950 Pi tyospovites pallidus Reissinger, p. 109, pi. 15 figs. 1-

1953 Caytonia onoodes Harris , Bolkhovitina, p. 113, pi . 20

figs. 207 a, b.

1955 Vitveisporites signatus Leschik, p . 53, pi. 8 fig . 10 .

1956 Conifevaletes impubevus Andreeva , p . 271, pi. 60 fig. 124.

1956 Conifevaletes stultulus Andreeva, p. 271, pi. 60 fig. 125.

1958 Vitveisporites pallidus (Reissinger) Nilsson, p. 78, pi. 7

figs. 12-14.

1958 Caytonipollenites pallidus (Reissinger) Couper, p. 156,

pi. 26 figs. 7, 8.

1959 Caytonipollenites subtilus de Jersey, p. 381, pi. 3 fig. 4

1960 Caytoniales Tchalyschev& Varyukhina, pi. 3 figs, la, lb.

1962 Vitveisporites subtilus (de Jersey) de Jersey, p. 11, pi. 4,

figs. 8, 9.

1964 Caytonidites alatioonfovmis Malyavkhina, p. 93, pi. 5 fig. 9.

1964 Caytonipollenites latus Maedler, p. 61, pi. 3 fig. 10

1964 Caytonipollenites veduotus Maedler, p. 61, pi. 3 fig. 11 - 265-

Dimens ions.

O.L. 23 (34) 43 microns - 20 specimens measured from sample 985.

L.C. 13 (21.5) 25 microns

L.S. 17 (23) 27 microns

Remarks .

Pollen referrable to Vitreisporites pallidus have been extracted from the caytonialean fructifications Caytonanthus arberi (Thomas), C. kocki Harris, C. onoodes Harris and an unnamed species of Caytonanthus associated with Sagenopteris colopodes Harris (Harris, 1964). Harris suggests that the intrareticulation of sacci of C. onoodes is more pronounced than that of C. arberi and that the sacci are somewhat larger

(Harris 1964 , p. 15).Potonie (1962a, pp . 151-152) suggests that these differences may be a result of the different stages of maturity of the material examined. It is probable that the forms assigned to V. pallidus represent a polyspecial grouping.

Previous records.

Vitreisporites pallidus has been reported from sediments ranging in age from Early Permian (Balme, 1970) to Eocene (Rei- ssinger, 1950). In N.S.W. it first appears as a very rare com ponent of Early Permian microfloras. It is a common component of most local Triassic, Jurassic and Lower Cretaceous microfloras.

Occurrence.

In the present study V. pallidus was a relatively rare component of Late Permian Newcastle Coal Measure microfloras.

It became common immediately above the Vales Point Coal Member and in other basal Narrabeen Group microfloras. It is a con- - 266- stant component of most microfloras from the Narrabeen Group,

Hawkesbury Sandstone and Wianamatta Group, although obviously less prominent in association with Lunatisporites.

Vitreisporites sp. 1

PI. 40 fig. 1, 2.

Description of specimens.

Pollen, bisaccate. Outline generally haploxylonoid, though often displaying a monosaccate tendency. Corpus circular to oval {l.o. usually slightly greater than b.o.), often with com pression folds arranged sub-parallel to the edges of the cappula.

Cappa thin, (about 1 micron), finely infrareticulate, extending over most of proximal surface of the corpus. Cappula fairly wide in specimens with well separated sacci, sides straight or slightly convex, exoexine apparently smooth and structureless.

Haploxylonoid forms display small sacci, set off proximal sur face of corpus, distally inclined. Tendency for exinal detach ment to continue laterally, which eventually results in a more or less monosaccate organisation sacci inf rareticulate .

Dimens ions.

O.L. 30 (39) 52 microns - Measured from distinctly bisaccate forms

B.C. 23 (28) 34 microns

L.C. 25 (30) 37 microns

B.S. 11 (14) 18 microns

L.S. 19 (22) 26 microns

Remarks.

Vitreisporites sp . 1 appears to display a continuous gra dation with forms tentatively identified as Suloosaooispora lata de Jersey & Hamilton. - 267 -

Comparisons.

Vitreisporites sp. 1 is distinguished from V. pallidus

(Reissinger) Nilsson by its smaller sacci (in distinctly bisaccate specimens), more obvious distal inclination of the sacci and the wider cappula. The cappula of V. pall-ictus is considered to have a characteristic biconvex shape.

Occurrence.

Vitreisporites sp. 1 was first recognised immediately below Vales Point Coal Member. It occurs intermittently through out the Narrabeen Group. It is a relatively consistent component of microfloras from the Hawkesbury Sandstone, Wianamatta Group and their equivalents.

Genus SULCOSACCISPORA Klaus 1964.

Type species. Suloosaooispora minuta Klaus - original desig

nation.

Suloosaooispora lata de Jersey & Hamilton

PI. 40 figs. 6, 7.

1967 Suloosaooispora lata de Jersey & Hamilton, p. 15, pi. 8

figs. 1-4.

Remarks.

Pollen grains indistinguishable from the specimens assigned to Suloosaooispora lata occur intermittently in the Hawkesbury

Sandstone, the Wianamatta Group and equivalent strata. I believe these forms are possibly variants of Vitreisporites sp. 1.

Genus MINUTOSACCUS Maedler 1964.

Type species. Minutosaoous doubingeri (Klaus) comb. nov. -

{Miorooaohryidites doubingeri Klaus 1964, p. 15,

pi. 3 , figs. 27 , 28.) - 268-

Maedler (June, 1964) designated M. aoutus as the type species of the genus Minutosaccus. However, Maedler's illus tration of M. aoutus is indistinguishable from forms illustrated by Klaus (April, 1964 , pi. 3 figs. 27 , 28) as Micvocachvyidites doubing eri.

Minutosaccus sp. 1.

PI. 40 fig. 8.

Description of specimens.

Pollen grains, bisaccate. Corpus circular to oval in polar view. No structure evident in corpus exoexine. Sacci very small, usually with pronounced distal inclination. Exo- exinal structure of sacci scarcely evident. Cappula usually dis tine t .

Dimensions .

O.L. 22 - 27 microns - 3 specimens measured from sample 522.

B.C. 19 - 21 microns

L.C. 19 - 22 microns

B.S. 8-11 microns

L.S. 15 - 19 microns

Occurrence.

Minutosaccus sp. 1 was encountered in two samples from the central portion of the Hawkesbury Sandstone.

Turma PLICATES Naumova 1937

Infraturma PRAECOLPATI Potonie & Kremp 1954

Genus PRAECOLPATITES Bharadwaj & Srivastava 1969, emend.

Type species. Pvaecolgatites sinuosus (Balme & Hennelly)

Bharadwaj & Srivastava. - 269- Remarks .

Bharadwaj & Srivastava (1969, p. 140) originally proposed Praeootpatites nidpurensis Bharadwaj & Srivastava, 1969 as the

type species of the genus, Praeootpatites. However, 1 regard

P. nidpurensis as a junior synonym of P. sinuosus CBalme & Hennelly) Bharadwaj & Srivastava.

Emended diagnosis. Pollen grains, ellipsoidal to oval in polar view. Distal surface exhibits three furrows (=colpi). The central furrow

parallels the long axis of the grain, the marginal furrows sub

parallel the sides of the grain. The furrows are separated by

two inflated ridges. Proximal surface is undifferentiated. Exine s truetured.

Remarks.

Bharadwaj & Srivastava (1969) interpret Praeootpatites as being characterised by three distal folds. However, the interpretable specimens which they illustrate, including the form they assign as holotype of the type species, display only two distal folds. Comp ar isons.

Sohop fipoitenites Potonie & Kremp 1954 is superficially

similar to Praeootpatites, but is interpreted as possessing

two distal furrows which are often accompanied by folds. Al

though Erdtman (1948) originally interpreted Euoommiidites troedssonii as tricolpate Hughes (1961) describes this genus as bearing a single distal furrow with a proximal ring furrow.

Eucommiidites is thus significantly different in organisation to Praeootpatites. -2 70-

I regard Bennettiteaepollenites (Thiergart) Potonie 1958 as synonymous with Euoommiidites although the relative priority of these taxa is still uncertain.

Praeoolpatites sinuosus (Balme & Hennelly) Bharadwaj & Srivastava

PI. 40 f igs . 9-15

Selected Synonymy.

1945 P3B - Dulhunty, p. 151, fig. l-3b.

1956a Marsupipollenites sinuosus Balme & Hennelly, p. 61, pi. 3

figs. 25-28

1962 Gnetaoeaepollenites sinuosus (Balme & Hennelly) Bharadwaj,

p. 99, pi. 5 fig. 92.

71964 Welwitsohiapites tenuis Bharadwaj & Salujha, p. 213, pi.12

figs. 164-165

1967 Gnetaoeaepollenites grandis Maheshwari, p. 277, pi. 9,

fig . 72

1969 Praeoolpatites nidpurensis Bharadwaj & Srivastava, p. 141,

pi. 29 figs. 117-124.

Description of specimens.

Pollen grains, ellipsoidal to oval in polar view. Distal surface exhibits three furrows separated by inflated exine ridges. Central furrow longest, often fusiform in shape, running parallel to long axis of the grain, occasionally exhibiting narrow, centrally located, exoexinal ridge. Furrows marginal to central furrow usually cresentic, running sub-parallel to the edges of the grain. Distal exine surrounding furrow appears to have been inflated and is particularly prone to folding, more or less parallel to the axis of the distal ridges. Proximal - 271- surface is usually undifferentiated. Exine distinctly infra- bacula te.

Dimens ions.

Long axis 50 (73) 95 microns. 20 specimens measured.

Short axis 25 (33) 46 microns.

Remarks.

Although they indicated the presence a monolete mark on the proximal surface of "Marsupipollenites" sinuosus 3 Balme & Hen- nelly otherwise accurately interpreted the morphology of the species. Recently, Balme (1970) reinterpreted this form as being polyplicate, with four to six heavy folds, each associ ated with a furrow. I have not found any evidence of this type of organisation in this material.

Previous records.

Praecolpatites sinuosus is characteristic of the Australian

Mid-Late Permian Dulhuntyispora Assemblage (Balme, 1964). It has been reported from the Beacon Group of Antarctica (Balme &

Playford, 1967). Bharadwaj & Salujha (1964) report its occur rence in the Raniganj Coal Measures of India whilst Balme (1970) indicates its occurrence in the Chhidru Formation of the Salt range.

Comparisons.

Bharadwaj & Srivastava (1969) indicates that P. sinuosus is differentiated from P. nidpurensis Bharadwaj & Srivastava by its smaller size. The validity of this distinction is questionable.

Occurrence.

Praecolpatites sinuosus occurs as a fairly constant but minor component of Mid-Late Permian coal measure microfloras. It occurs - 272- in basalmost Narrabeen Group microfloras, usually disappearing in the first 100 ft. of the sequence.

Infraturma POLYPLICATA Erdtman

Genus EPHEDRIPITES Bolkhovitina ex Potonie 1958

Type species. Ephedripites medioZobastus Bolkhovitina -

designated by Potonie 1958, p. 88.

Remarks.

Fossil pollen which closely resemble pollen of the Ephe- draceae have been assigned principally to three form genera.

These are Ephedripites Bolkhovitina ex Potonie 1958, Equiseto- sporites Daugherty emend. Pocock & Jansonius 1964 and Gneta- ceaepoZZenites Thiergart 1938. The relative validity of these genera has been examined by Pocock & Jansonius (in Pocock, 1964) and Balme (1970). Pocock & Jansonius reinterpret Equisetospo- rites in light of the investigations of Scott (1960), maintaining that it has precedence over the other genera, which they regard as invalid. The confusion concerning the holotype of Gnetaceae- poZZenites eZZiptieus Thiergart is cited and it is concluded that this particular specimen is too poorly preserved to allow accurate circumscription of the morphology. They cite the rejection of

Ephedripites by Bolkhovitina (iny(i959) as invalidating that genus.

Balme, correctly, points out that the holotype of Equisetosporites ohinZeana Daugherty is also extremely poorly preserved, so that it too is unsatisfactory as the basis of a genus. Balme recom mends the retention of Ephedripites on the basis the wide accep tance of this morphological concept of this form. Invalidity of the genus due to Bolkhovitina's 1959 rejection is refuted on -2 7 3- the basis that it was previously validated by Potonie (1958).

Ephedripites steevesi (Jansonius) de Jersey & Hamilton.

PI. 41 figs. 20-23.

71960 Ephedra sp. - Scott, pi. 1 fig. 7.

1962 Gnetaceaepollenites steevesi Jansonius, p. 77, pi. 15,

figs. 28-33.

1965 Gnetaoeaepollenites sp., McGregor, pi. 1 figs. 22, 25.

71966 Schizaeites sp. - Tschalyschev & Varyukhina, pi. 6, fig. 4.

1967 Ephedripites steevesi (Jansonius) de Jersey & Hamilton,

p. 19, pi. 9 fig. 7.

71968 Equisetosporites oaoheutensis Jain, p. 34, pi. 10, figs.

135, 136.

1968 Equisetosporites steevesi (Jansonius) de Jersey, p. 20,

pi. 2 figs. 6, 7.

Dimens ions.

Length 25 (31) 46 microns. 20 specimens measured.

Width 13 (17) 21 microns.

Remarks.

The Sydney Basin population assigned to Ephedripites stee vesi is marginally smaller than the Canadian assemblage described by Jansonius. They also display an average of 10 longitudinal ribs. In all other respects they conform to the type material.

Previous records.

Microfossils regarded above as synonymous with Ephedripites steevesi have been reported from the Late Triassic Chinle For mation by Scott (1960) . Jansonius (1962) indicates its occurrence in the Early Triassic of Canada. Identical forms are recorded - 274- from the Early Triassic Bjorne Formation of Ellesmere Island by

McGregor (1965). The line drawing of Tschalyschev & Varyukhina

(1966, pi. 6 fig. 4) suggests that morphologically similar forms occur in the Rhaetic of the Urals. This species occurs widely in the Bowen Basin, Queensland having been encountered in the

Clematis Sandstone (de Jersey, 1968), the Moolayember Formation

(de Jersey & Hamilton) and the Wandoan Formation (Helby - unpub lished reports). Similar forms are illustrated as Equisetospo- rites eaeheutensis from the Mid Triassic of Argentina by Jain

(1968).

Occurrence.

Ephedripites steevesi is first encountered in the lower portion of the Gosford Sub Group in the Balmain Shaft. It ex tends throughout the Hawkesbury Sandstone, Wianamatta Group and their equivalents as a common and characteristic microfloral component.

Genus WELWITSCHIAPITES Bolkhovitina ex Potonie 1958.

Type species. Welwitsehiapites magniolobatus Bolkhovitina -

designated by Potonie (1958, p. 89).

Remarks.

The generic concept of Welwitsehiapites Bolkhovitina ex

Potonie 1958 encompasses pollen grains with oval to ellipsoidal ambs, the exoexine being differentiated into a number of more or less parallel, raised ridges which may terminate abruptly, branch or join adjacent ridges converge towards the extremities of the grain, often projecting as an irregular exoexinal boss.

The genus Welwitsehiapites was informally introduced by - 275-

Bolkhovitina (1953, pp. 60-61) when she referred two formally described species to it. It was later validated by Potonie

(1958), who selected W. magnbolobatus Bolkhovitina as type species and presented a generic description. Bolkhovitina (in

Kremp, Ames & Kovar, 1959) subsequently attempted to reject the genus by recombining W. magniolobatus with the recent genus

Sohizaea Smith 1798 and W. alekhenii Bolkhovitina with the recent genus Aneimia Schwartz 1806. These recombinations are not accep table and Potonie is regarded as the publishing author of the genus Welwitschiapites.

The concept of Welwitschiapites as outlined by Potonie

(1958) is very close to the interpretation of Ephedripites Bol khovitina ex Potonie 1958. It would appear to differ in possess ing raised exoexinal ridges which branch or are joined to adja cent ridges by "bars". Potonie regards the laterally projecting exoexinal boss as diagnostic. Potonie interprets Welwitschites

Saklinskaya 1957 as a junior synonym of Welwitschiapites.

? Welwitschiapites australiensis sp. nov.

PI. 41 figs. 1 - 12.

Description of specimens.

Pollen grains, ? polyplicate, amb more or less oval although periphery invariably irregular. Exine layered with intexine and exoexine in close contact. Exoexine up to 2 microns thick (in cluding ridges), arranged in irregular ridges which are more or less aligned in the direction of the long axis of the grain.

Ridges branch, lateral branches usually joining adjacent ridges to form an elongate but very irregular reticulate pattern. Width - 276-

of ridges variable ranging from 1 - 2.5 microns, usually about

1.5 - 2 microns high. Junction of ridges often surmounted by

irregular node, projecting up to 2 microns above level of ridge.

Ridges converge laterally, projecting at the edge of the grain,

often merging to form an irregular boss. Exoexine not notice

ably structured, surface more or less smooth. Intexine appar

ently smoo th.

Dimensions.

Long axis 24 (34.5) 43 microns 35 specimens measured from

Short axis 19 (24) 27 microns sample 533.

Type Locality.

Wollongong D.D.H. No. 28 at 801 ft. (upper portion of

Grose Sandstone).

Holo type.

Slide 533/1 36.4 112.0 Illustrations PI. 41, figs. 9,10,

(32 x 22 microns) .

Remarks.

Although the arrangement of the exoexinal ridges of the

forms described above is considerably less regular than previ

ously described species, this species is considered to fall with in the concept of Wetwitschiapites. Comp a r i s ons . Welwitsohiapites magniolobatus Bolkhovitina has wider, more regular ridges which display only occasional branching. It lacks

the projecting nodes and consequently has a more regular outline than W. australiens is sp. nov. W. alekhinii Bolkhovitina dis plays a lesser degree of branching and is considerably larger

(110-120 microns). - 277-

0 cc ur r enc e.

Welwitschiapites australiensis sp. nov. was only encountered

in sample 533 which was located in the upper portion of the Grose

Sands tone.

Subturma MONOCOLPATES Wodehouse emend. Iverson & Troels - Smith

1950 .

Infraturma INTORTI Naumova emend. Potonie 1958.

Genus CYCADOPITES Wodehouse ex Wilson & Webster 1946.

Type species. Cycadopites follicularis Wilson & Webster -

original designation.

Synonymy.

Jansonius (1962, p. 80) has presented a fairly comprehen sive generic synonymy. To that list can be added:

1961 Punctamonocolpites Pierce, p. 47.

1968 Suloatopites Jain, p. 35

1968 Bharadwajapollenites Jain, p. 36

Remarks.

Balme (1970, p. ) in accepting Jansonius' treatment of

Cycadopites suggested that it should be restricted to forms devoid of exine sculpture or structure. This interpretation varies slightly from that of Jansonius who assigned "intra- punctate" specimens to Cycadopites cf. C. folliculatis Wilson

& Webster - the type species. I am inclined to accept Jansonius' interpretation.

Couper (1958, pp. 122 - 128) has discussed the in situ occurrence of a large number of grains of this general organi sation, indicating their polyphyletic affinities. These include - 278-

representatives of the Cycadales, Ginkgoales and Bennettitales

which range in age from Late Triassic to Lower Cretaceous. Town-

row (1960) extended this range by illustrating similar pollen

extracted from Antevsia Harris 1957, a Triassic member of the

Peltaspermaceae. Alpern et al. (1963, text fig. Id) indicate

that monocolpate forms similar to Cy cadopites range through the

Permian, possibly extending into the Late Stephanian. I am not

aware of "pollen" of this type which have been recovered from

Palaeozoic fructifications.

Cycadopites follicularis Wilson & Webster

PI. 40 figs. 13-19

Possible Synonymy.

1946 Cycadopites follicularis Wilson & Webster, pp. 274 - 275,

fig . 7 .

1953 Ginkgo typica (Malyavkhina), Bolkhovitina, pp. 62-63, pl.X,

fig. 3-4.

1955 Monocolpopollenites acerrimus Leschik, pp. 41-42, pi. 5

fig• 15 .

195 7 Entylissa nitidus Balme, p. 30,figs. 78 - 80.

1958 Monosulcites minimus auct. non. Cookson, Couper, p. 157,

pi. 26 fig. 23 - 25

?1959 Entylissia erassimarginatus de Jersey, p. 361, pi. 2

figs. 15, 16.

1962 Ginkgocycadophytus nitidus (Balme) De Jersey, p. 2, pi. 5

figs. 23 - 25.

?1962 Ginkgocycadophytus crassimarginatus (de Jersey) de Jersey,

p . 12 , pi. 5 fig . 4 . - 279-

1964 Cycadopollenites follicularis (Wilson & Webster), Danze-

Corsin & Laveine, in Briche, Danze-Corsin & Laveine, p. 108,

pi. XI, fig. 13.

1965 Cyoadopites avgentinus Herbst, p. 148, pi. 2 figs. 24-27.

?1968 Cyoadopites enormis Jain, p. 34, pi. 10 figs. 144-146.

1968 Sulcatopites bharadwajii Jain, p. 35, pi. 10 figs.149, 150.

1967 Sulcatopites cacheutensis Jain, p. 35, pi. 10 figs.151-153.

1968 Sulcatopites balmei Jain, p. 35, pi. 10 figs. 154-158.

Description of specimens.

See Balme 1970, p.

Remarks.

A broad interpretation of Cyoadopites folliculavis Wilson

& Webster has been presented by Balme (1970, p. ). Al

though the colpus often narrows in the vicinity of the polar

axis, the significance of this feature may be overrated. A

complete range of colpus shapes is illustrated on PI. 40, the

end members of this range possibly conforming more closely to

Monosulcites Cookson ex Couper 1953. Similarly, I have not been

able to interpret the significance in slight thickenings of

colpus edges. De Jersey (1959) and Jain (1968) regard this

feature as diagnostically important.

Previous records.

Balme (1970, p. ) indicates that forms which may be

assigned to C. follicularis range in age from Late Carboniferous

to Recent. In the Salt Range succession it extends from the

Early Permian Amb Formation through Lower Triassic. It is not

reported from the Tredian Formation. It is interesting to note - 280- that de Jersey (1968) has identified this species in the upper portion of the Rewan Formation of southern Queensland. These occurrences are in marked contrast to the situation in the Sydney

Basin where the form first appears in probable Mid Triassic s e d imen t s .

Occurrence.

Cyoadopites foUicutavis is not encountered below the base of the Hawkesbury Sandstone in the Sydney Basin. It is prominent throughout most of the Hawkesbury Sandstone and Wianamatta Group.

However, it is noticeably less common in equivalent sections to the north-west.

?Cyoadopites sp.

PI. 42 figs. 1-3.

Description of specimens.

Pollen, monocolpate. Amb oval to lense shaped. Colpus usually extends full length of the grain. In some specimens the colpus is scarcely open. Exine about 1 micron thick, smooth and apparently without structure.

Dimens ions.

Long axis 16 - 22 microns

Short axis 9-13 microns

Comp a r i s ons.

This form resembles Monosutoites minima Cookson, but is slightly smaller and in most specimens has a significantly larger long axis: short axis ratio. The illustrations of Mono- suloites minima Cookson (1947, figs. 47-50) suggest that the exine may be structured. (punctate). - 281-

Occurrence.

ICyoadop'ites sp. is a relatively constant but rare component of Wianamatta Group microfloras.

MICROPLANKTON.

A relatively diverse group of microfossils of uncertain origin occur intermittently through the Late Permian-Triassic sequence of the Sydney Basin. As my experience with these organisms is inadequate I have attempted to describe and illus trate only the broad morphographic features of the various populations. These microfossils are referred to the Group

ACRITARCHA Evitt 1963 and classified according to the system proposed by Downie, Evitt and Sarjeant (1963). Generic assign ments of forms not recognised as having been previously des cribed are regarded as tentative only.

The environmental significance of the Acritarcha as a whole is uncertain although Downie, Evitt and Sarjeant (1963, p.7) state "In general, the group is marine.." I believe that there is a close correlation between the occurrence of certain genera

(Veryhachium, Micrhystridium) and marine environments in eastern

Australian Permian and to a lesser extent Triassic sequences.

However, the significance of a number of other genera, more com monly associated with highly carbonaceous sediments, is yet to be d e t ermine d.

Group ACRITARCHA Evitt 1963

Subgroup ACANTHOMORPHITAE Downie, Evitt & Sarjeant 1963

Genus BALT ISPHAERIDIUM Eisenack emend. Downie & Sarjeant 1963. - 282-

Type species. Baltisphaeridium longispinosum (Eisenack) Eisenack

- original designation.

Baltisphaeridium sp. 1

PI. 42 figs. 44 - 46.

Description of specimens.

Microfossils, body circular in outline. Wall 1.5 - 2 microns thick, single layered, covered with scattered spines.

Spines 3 - 6 microns in length, 1-1.5 microns in basal diameter, usually tapered, up to 25 spines showing at the periphery.

Dimens ions.

Body diameter 21 (27) 37 microns - 10 specimens measured.

Comparisons.

Baltisphaeridium sp. 1 differs from Baltisphaeridium sp. 2 in having longer spines. It has a lesser number of shorter, more attenuate spines than Baltisphaeridium sp. 3. It has a longer body and a smaller spine length/body daimeter ratio than

Micrhystridium sp. 2. It resembles B. ehrenbergi var. brevispi- nosum (Deflandre) Sarjeant but has a thicker wall.

Occurrence.

Baltisphaeridium sp. 1 occurs intermittently in samples from the Wianamatta Group. It is slightly more abundant in the upper part of the section.

Baltisphaeridium s p . 2

PI. 42 figs. 39-41.

Description of specimens.

Microfossi1s, circular in outline. Wall 1.5-2 microns thick, covered with scattered spines 2-3 microns apart. Spines 1 micron basal diameter, up to 2 microns in length, usually tapered, al- - 283-

though some blunt processes do occur.

D imens io n s .

Body diameter 27, 31 microns 2 specimens measured.

Comparisons .

Baltisphaeridium sp. 2 differs from Baltisphaeridium s p . 1 and Baltisphaeridium s p . 3 in size and in the nature of the

spines. It is similar to Lophosphaeridium triangulatum Downie

(1963, pi. 92, fig. 1), but has slightly shorter spines and is possibly slightly larger.

Occurrence.

Baltisphaeridium sp. 2 occurs as a very rare component of microfloras in the Ashfield Shale, Bringelly Shale and Picton

Forma t io n .

Baltisphaeridium s p . 3.

PI. 42, fig. 38, pi. 43, fig. 6.

Description of specimens.

Microfossi1s, body circular to oval in outline. Wall single layered, 0.5-1 micron thick, covered with scattered spines about

6 microns apart. Spines up to 12 microns in length, 2-4 microns basal diameter, gently tapered. Spines commonly bent and broken.

Dimens ions.

Maximum body diameter 20 (26) 34 microns - 6 specimens measured from sample 963.

Comparisons.

Baltisphaeridium sp. 2 in the size nature and disposition of the spines. It has more numerous, larger spines than Miorhy- stridium s p . 3. - 284-

Remarks .

All specimens of Baltisphaeridium sp. 3 are relatively poorly preserved, as is the entire microflora of sample 963.

Occ ur renc e.

Baltisphaeridium sp. 3 occurs as a rare but distinctive component of the microflora in sample 963, taken about 100 ft. above the base of the Narrabeen Group in the Balmain Shaft.

Baltisphaeridium sp. 4

PI. 42 fig. 37.

Description of specimen.

Microfossils, body circular to oval in outline. Wall single layered, about 0.5 microns thick, covered with scattered spines 4-7 microns apart. Spines 2.5-4 microns long, tapering sharply from a very broad base, 11 and 13 spines visible at periphery.

Dimensions .

Body diameter 22, 24 microns - 2 specimens measured from s amp 1e 9 8 5.

Comparisons.

Baltisphaeridium sp. 4 has smaller, less numerous spines than Baltisphaeridium sp. 1 and Baltisphaeridium sp. 3. It has a thinner body wall and longer, less numerous spines than Baltis phaeridium sp. 2.

Occurrence.

Baltisphaeridium sp. 4 if a very rare component of the basal

Narrabeen Group microflora (sample 985).

Genus MICRHYSTRIDIUM Deflandre emend. Downie & Sarjeant 1963. - 285-

Type species. Micrhystridium inconspiauum (Deflandre)

Deflandre - original designation.

Micrhystridium sp. 1

PI. 42 figs. 7-18

Description of specimens.

Microfossil, circular in outline. Wall single layered,

0.5-1 micron thick, some (? larger) specimens exhibiting a smaller circular opening 2-3 microns in diameter. Wall covered with very closely packed projections, spines about 0.2 - 1 micron in basal diameter, up to 4 microns in length. Spines taper markedly above basal portion (about 1 micron), usually bent and often broken to give denticulate outline.

Dimens ions.

Body diameter 12 (18.5) 24 microns - 50 specimens measured from slide 985/4.

17 (21.5) 37 microns - 20 specimens measured from slide 986/2.

Remarks.

The nature of occurrence of the small, spinose acritarch - the micrhystridia (Downie & Sarjeant 1963, p. 84) suggests that their retention as a distinct generic unit is warranted. In emending the genus Micrhystridium Downie & Sarjeant (1963) indi cated that an arbitrary size limit of 20 microns should delineate that genus from Baltisphaeridium Eisenack emend. Downie & Sarjeant

1963. In the present study two separate populations of Micrhy- stridium sp. 1 exhibit mean diameters on either side of the arbi trary boundary between the genera. However, the mode of occurrence - 286-

(18% of total microfossil population in sample 985) suggest that this form should be assigned to Md crhy s t rdddum.

Comparisons.

Mdorhystrdddum sp. 1 is distinguished from Mdorhystrdddum sp. 2 by its larger mean size and finer, more densely packed projections. This form is very similar to Lophosphaerdddum pdlosum Downie but slightly smaller. The nature of the spines differentiate it from Baltdsphaerdddum sp. 1.

Occurrenc e.

Mdcrhystrdddum sp. 1 occurs abundantly in sample 985 above the Vales Point Coal Member in Newvale D.D.H. No. 28. It is less prominent in higher samples. This species is also encounter ed in lowermost Narrabeen Group sections intersected by N.S.W.

D.M. Wollongong D.D.H. No. 28, Camden D.D.H. No. 61, A.I. & S.

Appin D.D.H. No. 4, Central Coast Oil Terrigal D.D.H. No. 1 diamond drill holes and in the Balmain Shaft.

Mdcrhystrdddum sp. 2.

PI. 42 figs. 26-29.

Description of specimens.

Microfossil, body circular in outline. Wall 0.5 - 1 micron thick, frequently folded. Body covered with scattered spines, up to 18 spines showing at periphery. Spines about 1 micron basal diameter, up to 5 microns long, well tapered.

Dimens ions.

Body diameter 12 (15) 18 microns. 20 specimens measured from sample 482.

C omp aris on.

Mdcrhystrdddum sp. 2 differs from Baltdsphaerdddum sp. 1 - 287- by its smaller mean size and greater spine length/body diameter ratio. It is readily distinguishable from Veryhachium sp. 1 by circular body shape and attenuate nature of the spines.

Occurrence.

Micrhystridium sp. 2 is encountered intermittently through out the Wianamatta Group above the Mittagong Formation. It is particularly abundant in sample 482.

Micrhystridium sp. 3

PI. 42 fig. 30

Description of specimens.

Microfossils, body circular in outline. Wall single layered, about 1 micron thick, covered with scattered spines, laevigate or finely granulate between spines. Spines 6-10 microns in length,

1.5-2.5 microns in basal diameter, well tapered, often bent. 14 spines countered maximum on specimens examined.

Dimensions.

Body diameter 14 (17) 19 microns - 4 specimens measured.

Comparisons.

Micrhystridium sp. 3 differs from Micrhystridium sp. 2 in having coarser and less numerous spines. It is smaller and has finer, less numerous spines than Baltisphaeridium sp. 3.

Occurrenc e.

Micrhystridium sp. 3 is a rare component of microfloras occurring immediately above the Vales Point Coal Member in

Newvale D.D.H. No. 28 and microfloras of the Bringelly Shale.

Subgroup P0LYG0N0M0RPHITAE Downie, Evitt & Sarjeant 1963

Genus VERYHACHIUM Deunff emend. Downie & Sarjeant 1963. - 288-

Type species. Veryhachium trisuZcum Deunff (Name first published

by Deunf f p-954 pp. 305-30 6^] but type species not

validly described until 1958).

Veryhachium sp. 1

PI. 43 figs . 1-3.

Description of specimens.

Microfossils, body shape irregular due to projection of major spines. Overall outline star shaped to polygonal. Wall single layered, about 1 micron thick, laevigate to finely granu late. 6-8 major spines are irregularly scattered over the body and join it through broad bases. Spines usually tapered, 2.5-4 microns in length. A number of smaller spines 1-2 microns in basal diameter, 1-2 microns in length are scattered over the body in fig. 1, pi.43, these spines simulate a girdle. Most specimens display a large hole or tear in the wall of the body

( ? archeopyle) .

Dimens ions.

Body diameter 20 (24) 28 microns - 8 specimens measured.

Comparisons.

Veryhachium sp. 1 differs from Wilsonastrum colonicum

Jansonius by having a greater number of major spines and possess ing minor spines. The bristles described by Jansonius(1962, p.

88-89) were not observed. It differs from Verhachium sp. 2 by its larger size and number of major spines. The nature and number of spines differentiate it from Micrhystridium sp. 3 and

Baltisphaeridium sp. 3.

Occurrence.

Veryhachium sp. 1 occurs in samples 963, 985, 986 and 1006, - 289-

and is thus identified only from basal Narrabeen Group sediments.

Veryhaohium sp. 2

PI. 42 figs. 31-36.

Description of specimens.

Microfossils, body shape triangular to tetrahedral, sides markedly by convex. Corners drawn out into tapering spines,

usually three, but occasionally up to six. (PI. 42 fig. 33).

Wall single layered, o.5-l micron thick, laevigate. Spines pass

into the body through a very broad base, and vary from 2-4 microns

in length, sometimes broken.

D imens ions.

Body diameter 11 (13.5) 15 microns - 7 specimens measured from

s amp 1e 9 6 3.

C omp ar i sons.

This form is very similar to Witsonastrum oolonicum Janso- nius, but lacks the bristles which characterise that species. It is also smaller. It is smaller than Veryhaohium sp. 3 and

Veryhaohium sp. 4. It is similar to forms illustrated by Cramer

(1964, pi. 8, figs. 1-4) as Veryhaohium trispinosum (Eisenack).

I have encountered forms indistinguishable from this species in the roof sediments of the Main Lower Seam near Blackwater, Queens land.

Occurrence.

Veryhaohium sp. 2 occurred as a relatively rare component of the microflora in sample 963 about 100 ft. above the base of the Narrabeen Group in the Balmain Shaft.

Veryhaohium sp. 3

PI . 43 fig. 4. - 290-

Description of specimens.

Mierofossi1s , outline triangular, sides slightly convex.

Spines are drawn from each corner, three occurring on each speci men examined. Spines up to 10 microns long, tapered, contorted.

Wall single layered, 0.5 - 1 micron thick, laevigate.

Dimensions.

Body diameter 14, 14, 16 microns - 3 specimens measured from sample 391.

Comp a r i s ons.

This form differs from Wilsonastrum oolonicum Jansonius in having thin contorted spines. The bristles described by Janso nius (1962, p. 88, 89) were not observed. It has much longer spines than Veryhaohium sp. 2. It is smaller and has much finer spines than Veryhaohium sp. 4.

Occurrence.

Veryhaohium sp. 3 occurs as an extremely rare component of

Wianamatta Group microfloras. It is also encountered in the lower Narrabeen Group in the Balmain Shaft.

Veryhaohium sp. 4.

PI. 43 fig. 5.

Description of specimens.

Microfossils, outline triangular, sides slightly convex.

Spines are drawn from each corner, three occurring on each speci men examined. Spines 6-8 microns long, 2-3 microns basal diameter, gradually tapering. Wall single layered, 1 micron thick.

Dimens ions.

Body diameter 22 (26) 31 microns 2 specimens measured. - 291-

Comparisons .

Veryhachium sp. 4 is larger than Veryhachium sp. 3 and has heavier spines. It differs similarly from Veryhachium sp . 2. It is similar to Veryhaoh'ium trispinosum (Eisenack) Deunff.

Occurrence.

This form occurs as a very rare form in samples from about

100 ft. above the base of the Narrabeen Group in the Balmain

Shaft and the Liverpool Sub-Group of the Wianamatta Group.

Subgroup SPHAEROMORPHITAE Downie, Evitt & Sarjeant 1963.

Genus PILASPORITES Balme & Hennelly 1956.

Type species. Pilasporites calculus Balme & Hennelly - original

designation.

Remarks.

As defined by Balme & Hennelly Pilasporites can be inter preted to encompass smooth to granulate, punctate to reticulate organic walled bodies without visible germinal or dehiscence apparatus. Potonie (1960, p. 84) suggests that Pilasporites could be distinguished from Inap erturopollenites ex Thompson

& Pflug emend. Potonie 1966 and Psomosphaera ex Naumova emend.

Potonie 1958 by its thicker wall, but assigns all three genera to Psilonapiti. De Jersey (1962, p. 14) also refers to Pila sporites as a pollen. Similarly Jain (1968, p. 42) in emending the genus interprets it as being/monoporate pollen. However, it is extremely difficult to reconcile Jain's interpretation with the type material.

The occurrence of Pilasporites in large numbers in asso ciation with microfossils such as Peltacystia Balme & Segroves - 292-

1966, Tetraporina (Naumova), and Circulisporites de Jersey, 1962 suggests that it is probably of non-vascular origin. It is par ticularly abundant in Lower-Mid Permian carbonaceous sediments in the Sydney Basin.

Pilasporites calculus Balme & Hennelly

PI. 42 fig. 43.

Description of specimens.

See Balme & Hennelly (1956a, p. 64).

Remarks.

Pilasporites calculus is particularly common in carbonaceous sediments of the Permian age in the Sydney Basin.

Occurrence.

Pilasporites calculus occurs as a relatively rare component of microfloras in the vicinity of the Vales Point Coal Member in

Newvale D.D.H. No. 28.

Pilasporites plurigenus Balme & Hennelly

PI. 42 figs. 4-6.

Description of specimens.

See Balme & Hennelly. (1956a, p. 64).

Dimens ions.

Diameter 12 (-14.5) 17 - 50 specimens measured.

Remarks.

This form is most abundant in coal or other highly carbon aceous sediments.

Occurrence.

Pilasporites plurigenus is a common component of microfloras immediately above the Vales Point Coal Member in Newvale D.D.H.

No. 28. It is also prominent in carbonaceous and coaly samples - 293-

from the Liverpool Sub-Group.

Subgroup HERKOMORPHITAE Downie, Evitt & Sarjeant 1963.

Genus CYMATOISPHAERA Wetzel emend. Deflandre 1954.

Type species. Cymatiosphaera radiata Wetzel

? Cymatiosphaera sp.

PI. 42 fig. 19-25.

Description of specimens.

Microfossil with prominent opening ( ?archeopyle) . Outline

circular, slightly irregular or almost polygonal. Original shape probably spherical. Body wall is less than 1 micron thick,

apparently single layered, smooth to finely granulate. Surface of body wall divided into an irregular number of polygonal fields by folds. Folds stand 1-2 microns above general level of the body surface. A large opening is evident in most specimens. The opening is circular or may be polygonal in specimens in which the wall is strongly folded. Opening varies in size from 1/2 to 2/3 body d i ame ter.

Dimens ions.

Diameter 19 (25) 32 microns. 25 specimens measured from slide

986/2 .

Remarks.

The forms described above conform more or less to the con cept of Cymatiosphaera as emended by Deflandre (1954, p. 57).

There is however, no evidence of an opening in the body wall of

Cymatiosphaera and the polygonal fields are usually separated by a thin projecting membrane rather than folds. This species occurs in swarm proportions in sample 986 and is associated in - 294-

all cases with acritarchs and other microfossils of probable non-vas cular origin, suggesting that it almost certainly has non-vascular affinities and is possibly best referred to the acri tarcha.

Occurrence .

? Cymatiosphaera sp. is confined to the basal portion of the Narrabeen Group, occupied by the lower zonule of the Proto- haploxypinus retieulatus Assemblage.

Subgroup SCHIZOMORPHITAE Segroves 1967

Genus PELTACYSTIA Balme and Segroves 1966.

Type species. Peltaoystia venosa Balme & Segroves - original

designation - (p. 26).

Peltaoystia venosa Balme & Segroves.

PI. 43 figs. 12-17.

Description of specimens.

See Balme & Segroves (1966, p. 27).

D imens ions .

Equatorial diameter 36 (43) 50 - 7 specimens measured from sample 986 . 30 (42) 50-7 specimens measured from sample 985 . 42 (48) 59-9 specimens measured from sample 1006 .

Remarks.

The Peltaoystia venosa specimens occurred predominantly as detached halves. They were relatively poorly preserved and did not take up Safranin 0 stain. The presence of two distinct (see

Dimensions above) size assemblages suggests that these specimens are not reworked despite their relatively poor (relative to spore preservation) preservation. Balme & Segroves (1966, p. 27) indi- - 295- cate that these forms are probably unicellular members of the

Chlorococcales. They have also commented on the abundant occur rence of Peltaoystia in coals and closely associated clastic sediments together with large numbers of other microfossils of probable non-vascular origin such as Pilasporites Balme & Hen- nelly, Tetraporina (Naumova) and CircuZisporites (de Jersey).

They also suggest that an abundance of Peltacy s tia may be taken to characterise continental, fresh or brackish water sediments.

Peltaoystia venosa is common in three samples from Newvale D.D.H.

No. 28 where it is associated with large numbers of Mi orhy s tridium sp. 1 and ? Cymatiosphaera sp. together with Tetraporina sp.

Baltisphaeridium spp . , Veryhachium sp., Circulatisporites parvus

(de Jersey) Norris and Pitasporites pturigenus Balme & Hennelly.

These associations are interpreted as representing quiet, shallow brackish/marine conditions.

Occ urrenc e .

Pettaoystia venosa was a common component of microfloras in samples 986, 986m 1006 representing a 3 ft. interval immedi ately above the Vales Point Coal Member in Newvale D.D.H. No. 28.

It was also encountered in lower Narrabeen Group sediments in the

Balmain Shaft and Wollongong D.D.H. No. 28 and A.I. & S. Appin

D.D.H. No. 4.

Genus CIRCULISPORITES de Jersey emend. Norris 1965

Type species. Ciroulisporites parvus (de Jersey) Norris -

original designation.

Ciroulisporites parvus (de Jersey) Norris.

PI. 43 figs. 7-10 296-

Dimensions .

Diameter 14 (19) 27 microns - 20 specimens measured from sample

985 .

Diameter 18 (20) 24 microns - 20 specimens measured from sample

1005 .

Remarks.

Specimens of Cirout-isporites parvus in sample 985 occur predominantly as isolated halves (90+%). This sample is rela tively well preserved and has been very slightly over oxidised

(relative to other samples) with Schultze solution. Specimens occurring in sample 1005 occur predominantly (90%) as complete microfossils, although the process of dehiscence is usually underway. This sample is well preserved and relative to other samples is slightly under oxidised. Circulisporites parvus is reported from Permian of W.A., M-U Triassic of Queensland, L.

Permian-Triassic in N.S.W., M-U Triassic of Antarctica. Cireu- lisporites parvus occurs intermittently throughout the section, and is most prominently associated with richly carbonaceous sediments.

Subgroup uncertain.

Genus TETRAPORINA Naumova emend. Naumova 1950.

Type species. Tetraporina antiqua Naumova (designated by Potonie 1960, p. 130).

Remarks.

As defined by Naumova Tetraporina is characterised by the presence of four pores. However, Playford (1963, p. 658) points out that these pores are "... often either incompletely or not developed." Similarly, Segroves (1967, p. 302) indicates that - 297- pores are often simulated by arcuate folds. None of the speci mens described below display distinct pores.

Tetraporina sp. cf. T. horologia (Staplin) Playford

PI. 43 figs. 18. 19.

1960 Azonotetraporina ? horologia Staplin, p. 6, pi. 1, figs.4-6.

1963 Tetraporina horologia (Staplin) - Playford, p. 659, pi. 95

fig . 14, 15.

Description of specimens.

Microfossi1s, outline more or less quadrilateral. Dehi scence mechanism not apparent. Sides concave, corners rounded without any pore, although occasional arcuate folding occurred.

Wall apparently single layered, about 1 micron thick, laevigate.

Dimens ions.

Diameter (not diagonal) 19 (25) 30 microns - 8 specimens measured

Remarks.

All specimens examined were partially corroded. They are referred to Tetraporina horologia on the basis of their close similarity to specimens illustrated by Playford (1963, pi. 95, fig. 14). T. horologia has been reported from the Lower Carbon iferous of Canada and Spitsbergen. It also occurs in Permian and Triassic sediments in Western Australia.

Occurrence.

This form occurs as a rare component in microfloras imme diately above the Vales Point Coal Member in Newvale D.D.H. No.28

Tetraporina sp.

PI. 43 figs. 22, 23.

Description of specimens.

Microfossils, outline more or less quadrilateral, with one - 298- axis slightly longer than the other. Sides straight or convex, seldom concave, corners slightly rounded, several specimens exhi biting inflated projections from the corners up to 8 microns long and 6 microns wide (see PI. 43 fig. 23). Wall 1-2 microns thick, laevigate (although often extensively corroded).

Dimensions.

(not diagonal) 42x 36, 62x 56 microns - 12 specimens measured.

Remarks.

It is noted that the arcuate folds described by Segroves

(1967, p. 302) would probably result from deflation of the corner projections described above.

Occurrence.

This form is a relatively rare component of samples 985,

986 and 1006, immediately above the Vales Point Coal Member, in

Newvale D.D.H. No. 28.

Genus QUADRISPORITES Hennelly 1958.

Type species. Quadrisporites horridus Hennelly - original

des ignation.

Remarks.

Potonie & Lele (1961, p. 25) proposed an emendation of

Quadrisporites Hennelly 1958 suggesting that the tetrad concerned was rhomboidal rather than tetragonal. I believe that this emendation is based on confusion of the words tetragonal and tetrahedral by those authors. Segroves (1967) has suggested that Quadrisporites could be appropriately placed in the Acritar- cha. This is supported by the "swarm" like mode of occurrence of Quadrisporites and its close association with other non- - 299- vascular forms in Late Permian sediments in eastern Australia.

Quadrisporites horridus Hennelly

PI. 43 figs. 20, 21.

Selected Synonymy.

1946 Spore 23 (partim.) Virkki, p. 129, text fig. 39, pi. 6

fig. 71.

1958 Quadrisporites horridus Hennelly, p. 365, pi. 5, fig. 6, 7.

Description of specimen.

See Hennelly 1958, p. 365.

Dimens ions.

21 (32) 49 microns. 100 specimens measured from samples

627 and 628.

Holo type.

Although Hennelly (1958, p. 366) designated a type locality

(Appin D.D.H. No. 4 at 1697 ft. 2 inches) a holotype was not assigned. Potonie & Lele (1961, p. 25) have indicated the speci men illustrated by Hennelly on pi. 5 fig. 7 as lectotype ("Gene- ro typ e" ) .

Remarks .

Quadrisporites horridus Hennelly is reported as a rare component of carbonaceous sediments of Early Permian age from

India (Potonie & Lele, 1961), Pakistan (Virkki, 1946; Balme, 1970) and Australia (Segroves 1967; Helby - unpublished information.)

It is also recorded from the "assise a couches de houille" of the Belgian Congo to which H«$eg & Bose (1960) assign an Upper

Permian age. It occurs in basalmost Narrabeen Group sediments of the Sydney Basin (Hennelly, 1958) and is also encountered in - 300- the Late Permian Chhidru Formation of the Salt Range (Balme, 1970).

Helby & McElroy Cin press) have recently reported its occurrence from the Lashly Formation of the Beacon Group, Antarctica. Des pite its rather wide range of occurrence in Permian (and possibly

Triassic) sediments, the abundance of Q. horridus at the base of the Narrabeen Group and equivalent horizons throughout eastern

Australia constitutes a distinct and important stratigraphic horizon. At this horizon Q. horridus is associated with acritarchs and a number of other microfossils of probable non-vascular origin.

Occ urrenc e.

Quadrisporites horridus was not encountered in coal measure microfloras in the present study. It first appeared in basalmost

Narrabeen Group sediments, often in extreme abundance. It occur red intermittently throughout the lower portion of the Narrabeen

Group. Rare specimens have been encountered in several samples from the Wianamatta Group.