Terrestrial Palynology of Cape Roberts Project Drillhole CRP-3, Victoria Land Basin, Antarctica
'Institute of Geological & Nuclear Sciences. P.O. B o x 30368 Lower Him - New Zealand
^ B y d Polar Research Centcr. O h i o Skalc Universily. Colurnbus. O H 43210 - U.S.A.
Received 2 April 2001: accepted in revisedform 1 September 2001
Abstract
-
Sparse low diversity early Oligocene spore-pollen assemblages abovec'. 4 1 0 mbsf (metres below s e a floor) in CRP-3 arc dominated by Not11ofagn.s pollen. and a r e very s i m i l a r in c o m p o s i t i o n to those f r o m the lower part of CRP-2A. Anther-derived pollen aggregates. and a A~otli(;f'c;g~is leaf at 44.12 mbsf show that the palynomorphs were derived from vegetation growing at the time of deposition. This woody vegetation included several species of Not/~(~fcigns and podocarpaceous conifers. a few other angiospenn families. and few cryptogams except for bryophytes. I11 favourable sites the vegetation may have comprised a low scrub or closed forest intermediate in stature and floristic richness between that of
the Eocene and the limited vegetation of the late Oligocene to early Miocene. It may have been similar to A~o~hofogus woodland of the present-day Magellanic region. with summer mean daily temperatures at sea level of c. 10-12OC. M o r e stunted vegetation would have existed in exposed and upland sites. Wetland vegetation appears to have been minor. although Coptospora may in part represent a mire cominunity.
Below c. 410 mbsf samples are mostly barren, probably due to non-deposition of fine particles and dilution by high sediment deposition. A meagre but relatively high diversity assemblage at 781.36 mbsf contains Ccisiicirinci-type pollen, unknown in the higher CRP sequence but present in Eocene strata of CIROS-1 and glacial erratics of the M c M ~ i r d o Sound region. This limited data is consistent with Eocene dating of basal CRP-3 Cenozoic sediments from magnetostratigraphy.
INTRODUCTION
Cape Roberts P r o j e c t drillhole C R P - 3 , sited 11.76 km offshore from Cape Roberts at 77.0106' S and 163.6404' E (see location map), was drilled from annual sea-ice in the Ross Sea during the period 9 October to 19 November 1999. This third and final drillhole of the Cape Roberts Project completed a programme to obtain continuous core from Cenozoic and possible older strata on the western margin of the Victoria Land Basin. in order to investigate the early h i s t o r y of the A n t a r c t i c i c e sheet and Antarctic climate, and to elucidate the history of rifting of the A n t a r c t i c continent a s recorded by uplift of the Ti-ansantarctic Mountains and formation of the basin (Cape Roberts Science Team [CRST]. 2000).
Cape Roberts drillholes CRP- 1 and CRP-2/2A provide a sedimentary record that spans the Early O l i g o c e n e to E a r l y M i o c e n e , and terrestrial palynomorphs r e c o v e r e d f r o m t h e s e cores have e n a b l e d reconstruction of at least part of the contemporaneous vegetation (CRST 1998b, 1999;
Raine, 1998; Askin & Raine, 2000). A preliminary survey of terrestrial and marine palynological results from CRP-3 was provided in the Initial Report for this drillhole (CRST, 2000). In this paper we discuss
Cenozoic spores and pollen (collectively termed miospores), including results from study of additional s a m p l e s , and illustrate ecologically o r stratigraphically-important taxa. We have not at this s t a g e attempted an integrated account of t h e taxonomy and palaeoenvironmental significance of the complete Cape Roberts Cenozoic iniospore sequence.
The reader is referred to the Initial Report for a fuller account of redeposited palynomorphs derived from Permian to Triassic strata of the Beacon Supergroup and Jurassic sedimentary strata interbedded i n volcanics of the Ferrar Group, which are also present throughout the CRP-3 Cenozoic section. Cenozoic marine palynomorphs from CRP-3 are also discussed in the Initial Report (CRST, 2000, p. 147-158) and in a paper by Hannah, Wrenn & Wilson (this volume).
STRATIGRAPHY
A summary stratigraphic column for CRP-3 is included in figures 1 and 2. Water depth at the CRP-3 drillsite is 295 m, and core was obtained from c. 2.8 metres below sea floor (mbsf) down to the total depth at 939.42 mbsf, with overall core recovery of 97%.
The site was selected to overlap the lower Oligocene strata cored in nearby CRP-2/2A, but consensus of
"Corresponding author (i.1-aine@gns.cri.nz)
J . I . Raine & R./\. Askin 390
Metres
Earl!
Miocene
- ?
-Late Oligocene
-
?
-
Early Oligocene
- -
Late Eocene
Devonian
Sequences of
mudstone
---
sandstone, p
diamictite, A A
conglomerate - - - *
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.
... * - -...
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(mbsf) unconformities Tephra
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Outsize clasts 0.1 - 0.5 m---...--- ... . . .
. . . ... 330 - .
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Dolerite conglomerate
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Fig. 1 - Composite log from drillholes CRP-l. 2A and 3. Data are f r o m Cape Roberts Science Team ( 1 9 9 8 ~ . 1999 & 2000): w i t h stratigraphic ages adopted for this report.
magnetostratigraphic, biostratigraphic, lithologic, and seismic data suggests there is a gap of a few tens of metres between the two sections (CRST, 2000: 187- 1 8 9 ) . C e n o z o i c s t r a t a w e r e c o r e d d o w n t o 8 2 3 . 1 1 m b s f , a n d i g n e o u s - i n t r u d e d D e v o n i a n sandstones of the Beacon Supergroup from there to
the base of the hole. The Devonian rocks h a v r s o h r p r o v e d ulifossiliferous, and dating is b : i s r d o n pctrograpliic comparison with similar rocks c r o p p i ~ ~ y out in t h e Transantarctic Mountains. B a s a l post Beacon strata comprise a thin sandstone brcecia ;nu1 c o n g l o m e r a t e interpreted as a subaerial taluh or alluvial fan deposit (lithostratigraphical un i l
1
l ,S H1
5 . 3 ) , followed by dolerite conglomerate a n d min01, sandstone up to c. 790 mbsf (LSU 15.2 to lower LSU
3 . 2 ) , considered to have been deposited by ii liigli gradient fluvial system. Above this level. s;i~ii.lsloiu~
and c o n g l o m e r a t e sedimentation continncil i n ; I
marine setting, possibly deltaic and probably rapidly deposited below c. 3 3 0 mbsf ( L S U 1 3 . 2 to 9 . 1 ) .
Above 330 mbsf strata also include n i ~ i d s t o ~ i c , i i n d
diamictite of more unequivocally glacio~~iarint-! origin, deposited in an inner shelf setting. This I':icies is similar to that seen in the lower part of CRP-212A.
The distribution of fossils in tlie Cenozoic section follows that of the mud component of the sediinenis.
and strata are for the most part poorly fossiliferous below the upper c. 200 111 of tlie core. In t h e iippi'i.
c. 200 m. dating is based on siliceous microfossils and calcareous nannofossils combined with magneto..
stratigraphy, and indicates that the top of t h e section lies in the mid-part of magnetochron C12r, i.e. i n ilie Early O l i g o c e n e , in accord with d a t i n g of the lowermost part of the CRP-212A section. Below this level t h e s e f o s s i l s a r e absent. and a l t h o u g h foraminifera, marine macrofossils, and marine a n d terrestrial palynomorphs occur consistently clown to c. 330 mbsf, and sporadically to near the base of the Cenozoic section, the biostratigraphic utility of these groups is low and dating is based on a count-back of magnetocl~rons. On this basis, and taking into account likely sedimentation rates, a zone of predominantly reversed magnetic polarity in the lower part of the s e c t i o n , u p t o c. 6 3 0 rnbsf, is at least a s old as magnetochron C13r and therefore Late E o c e n e or o l d e r ( F l o r i n d o e t a l . , t h i s volume) a l t h o u g h dinoflagellate workers prefer an age no older than uppermost Eocene (Hannah & Fielding et al., this volume).
PALYNOLOGICAL PROCESSING
Palynological sample preparation followed the techniques described by the C a p e Roberts Science Team (1998a) and in more detail by Simes & Wren11 ( 1 9 9 8 ) . A l l p r e p a r a t i o n w a s p e r f o r m e d at t h e McMurdo Station laboratory during the 1999 drilling season, samples being assigned "P" prefix laboratory numbers in sequence with those of previous C R P d r i l l h o l e s . B e t w e e n 5 a n d 1 5 g of r o c k w e r e p r o c e s s e d f o r e a c h s a m p l e . S a m p l e d i g e s t i o n in hydrochloric and hydrofluoric acid using a ProLabo M401 microwave apparatus was followed by seven minutes oxidation with concentrated nitric acid. and decanting u s i n g a swirling method. Most samples were sieved through a 212 win mesh sieve to remove
Terrestrial I'alynology o f Cape Roberts Project Drillhole ('RI'?
Number of Cenozoic Total count miospore species Cenozoic miospores
Total count BeaconIFerrar miospores
Fig. 2 - Summary diagram showing the distribution of terrestrial palynomorphs in CRP-3. Species diversity of Cenozoic miospores is expressed as numbers of taxa identified in samples. Total abundance of Cenozoic and of redeposited Beacon Supergroup and Ferrar Group
~ i ~ i o s p o r e s (Permian to Jurassic) is based on counts of all specimens encountered in samples (which were of approximately equal size and completely examined). Columns on the left include age (see text). lithostratigraphic units (e.g. 1.1). and lithologic column as described in CRST (2000). F = fault.
c o a r s e mineral grains a n d other d e b r i s . T h o s e containing significant detrital coal fragments were passed through a 125 ~ i n i sieve. Sieved residues were further cleaned of unwanted mineral matter by heavy liquid separation with sodium p o l y t ~ ~ n g s t a t e ( 2 . 3 specific gravity). The final step for most organic rcsidues was sieving o n a 6 pm mesh cloth using a Vidal Filter apparatus (Raine & Tremain. 1992) to remove fine particles. Strew-~iiount microscope slides were made with glycerin jelly medium. Palynological slides for the C a p e Roberts Project clrillholes are d e p o s i t e d with the National P a l a e o n t o l o g i c a l Collection at Institute of Geological and Nuclear Sciences, Lower Hutt, New Zealand.
RESULTS
Palynology in the Initial Report was based upon examination of a total of 120 samples, including all ''fast-track" samples and additional samples to secure a s a m p l e s p a c i n g of c . 1 0 m o r less t h r o u g h t h e Cenozoic section. Results from a further 6 4 samples h a v e been i n c o r p o r a t e d in this p a p e r (Tab. 1).
including all palynological samples collected from below c. 350 mbsf. A further 24 samples prepared from the upper part of the core remain to be studied, h o w e v e r t h e new work has s o f a r c o n f i r m e d palynofloral trends previously reported.
RECYCLED AND CONTAMINANT PALYNOMORPHS
Within t h e C e n o z o i c s e c t i o n , both p r e s u m e d contemporaneous and recycled components can be recognised on the basis of preservation s t a t e and known stratigraphical range. The recycled component includes a few Cenozoic forms but mainly comprises Permian to Mesozoic miospores. Preservation of the C e n o z o i c p a l y n o m o r p h s , i n c l u d i n g p r e s u m e d contemporaneous and recycled specimens, is generally good to very good. There are some poorly preserved specimens, however, that are broken and torn, or have scarring from authigenic pyrite crystal growth. T h e Cenozoic specimens are mostly light yellow to yellow i n colour, a l t h o u g h s o m e have a d a r k e r ( y e l l o w - orange) hue. Recycled Permian and lower Mesozoic spores and pollen occur throughout much of CRP-3.
These miospores, which originate from the Beacon Supergroup and sedimentary interbeds of the Ferrar G r o u p v o l c a n i c s , c a n b e d i s t i n g u i s h e d by t h e i r distinctive morphology, and usually d a r k e r exinal c o l o u r ( y e l l o w - o r a n g e t h r o u g h b r o w n t o b l a c k ) relative t o t h e l i g h t yellow c o n t e m p o r a n e o u s miospores.
The extent of reworking of Cenozoic (or possible Late Cretaceous) spores and pollen from older rocks appears to b e less than in the upper part of C R P - 212A. N o t i c e a b l y d e e p e r y e l l o w s p e c i m e n s w i t h adherent organic matter, identified as P e n i n s ~ ~ l a p o l l i s
c/'. (177.76 mbsf, Pig. 4s) aiul T r i c o h i . i t i ' , s iiiicncstriiitii'i ( 8 3 . 0 2 mhsf. Figs. 4t. h ) a r c confidently considered to be redepositcd. Botli spt.\i.'ics were reported I'rom thc lower section o f CIROS I by Mildenhiill ( 1 9 8 9 ) . Rare s p e c i m e n s of /'. , q / / / i i , considered to possibly be rcdeposited. were obscrvi.~l i n the McMurdo Sound Eocene erratics h y Askin (2000). I n Australasiii. .'f g i l l i i has a range o f I.;itr Crctticeous to Eocene (Dcttmann & Jarzen, l <)SS), ; i n d
. .
I . pu'nvstria/n,s of Eocene to Pliocene ( S t o v c r K.Partridge. 1973: Macpliail 1999). Rare ~ C C L I I T C I ~ C ~ S of the g y m n o s p e r m s , D i l w y n i t e s grciniilain..\, Microcacln~~ic/i/c~.v diituirticus. and Tiichotonio,sii/(~//(~.\
s u ~ r a n i i l à § t ~ . ~ which o c c u r in samples t h a t liiel\
abundant a n d presumed c o n t e m p o r a n e o u s Notl~o/hgidites, are similar to sporadic occurrences ill CRP-1 a n d CRP-212A, a n d a r e a l s o l i k e l y to I-ic recycled s p e c i m e n s . S o m e of the f e r n spore specimens may also be recycled. as these occur i n only a few samples.
Specimens of Asteraceae (Tubuliflorae) pollen were encountered at 781.36 and 797.88 mbsf. These lack protoplasm, and may be fossil. Mildesihall ( 1989) recorded several similar specimens in the lower pan of the CIROS-1 sequence, tentatively regarding these as c o n t a m i n a t i o n . P o l l e n of the A s t e r a c c a e (= Compositae) family. which are common weeds and thus potential laboratory contaminants, first appears in Australasian s e q u e n c e s in t h e l a t e O l i g o c e n c (Pocknall & Mildenhall, 1984), but possibly earlier DSDP Site 254 in the Indian Ocean (Kemp & Harris.
1977). Recovery of further specimens is required to confirm the fossil nature of the CRP-3 and CllXOS-1 specimens.
MIOSPORE ABUNDANCE
Specimen counts presented in tables l a and I b result from study of the entire organic residue from palynological processing. Since the weight of sample processed was fairly uniform, usually 10 g in the section above c. 380 nibsf, and 10 to 20 g below that level, total counts are a reasonable guide to sample- to-sample variation in miospore abundance (Fig. 2).
This varied from moderate ( > l 0 0 specimens110 g), through low (10 to 100 specimens110 g), to sparse ( < l 0 specimens110 g) o r nil. We also examined 6 samples from the Beacon Supergroup section below 823.11 mbsf. Consistent with the coarse grain size and oxidising palaeoenvironment represented, these proved to be barren of palynomorphs or other organic material.
T h e Cenozoic section can be divided into three i n t e r v a l s on t h e b a s i s of C e n o z o i c m i o s p o r e abundance. The lowest interval, from the base up to c. 410 mbsf, is characterised by long barren intervals and sporadic sparse occurrences. From c. 410 mbsf up to c . 200 mbsf short intervals of sparse to low abundance alternate with barren intervals of similar thickness. Above c. 200 mbsf, Cenozoic miospores
Terrestrial Palynolo:y o f Cape Roberts Project Drillhole C K I ' - f 393
o c c u r i n ; i l l s a m p l e s . with abundance r e a r l i i n r mode~xtc l(-vels in a few samples. Highest ;ihiiiid;inccs occur i n iiiudstones and sandy n ~ ~ i d s t o n e s at 106.22 mbsf (cotint of 108. LSU 2.2). 114.90 nibsf (coimt 224. LSII 2 . 2 ) . 13 1.17 mbsf (count 72. I.SU 3. l ) , 190.77 nihsf (count 416. LSU 6.1 ). and 225.1 I mbsl (count 250. LSU 7.2). These abundances exceed those seen i n ('RP-1 and CRP-212A. tlie most similar
be in^
a count o f 6 4 miospores in mudstone at 575.36 mhsf i n the lower part of CRP-2A.
Peaks in recycled BeaconIFerrar niiospore o c c ~ ~ r r c i ~ ~ ~ s correspond in a general way with many of the peaks in occurrences of contemporaneous specimens, and correspond to finer sediment grainsizc.
Below 4 1 0 nibsf. w h e r e c o n t e m p o r a n e o u s p a l y n o ~ i i o r p h s a r e s p a r s e o r a b s e n t , peaks in abundance may also be d u e to recycled clasts of palynologically-rich sediment. The general rarity of Cenozoic miospores in the lower part of the CRP-3 core is believed to result from, in part. removal of the fine fritction of tlie sediment by winnowing and. in part, dilution by rapid influx of sediment. Sparseness of vegetation in the surrounding landscape could also have contributed to the low abundance of miospores.
COMPOSITION OF ASSEMBLAGES
Diversity varies in concert with total abundance of miospores (Fig. 2). being higher in tlie samples with greater abundance. but in general is low. Relatively high total counts in the upper c. 410 m of the core are niostly due to high levels of Nof11c~fc1gIcliies spp..
particularly of N. lc~chlaniae and in differentiated fusca group species. Other relatively abundant taxa include N. f l e m i n f i i . N . c f . flemingii. and various s p e c i e s of P o d o c a r p i d i i e s . A g g r e g a t e s of Notliofaeiclites lachlanicie and Nofhofagiclites fiisca g r o u p pollen grains (e.g. Fig. 411) occur at 101.59.
1 14.90. 1 3 1.17 and 225.1 1 mbsf. in association with h i g h counts of individual s p e c i m e n s . Mildenhall (1989) observed similar aggregates of Nofhofogiciifes pollen in CIROS-1. As suggested by Mildenhall. such aggregates are very likely to be due to incorporation of anthers in the sediment. Their fragility suggests that they are not recycled but transported. with very little disruption. from contemporaneous vegetation.
T h i s is supported by t h e p r e s e n c e o f a leaf of Nothofag~ls found in the CRP-3 core at 44.12 nibsf (Cantrill, this volun~e).
I n the upper c. 4 1 0 ni of c o r e , t h e taxonoinic c o m p o s i t i o n of t h e f l o r a i s very s i m i l a r to that encountered in the lower part of C R P - 2 A . with a similar number of species and few different species b e i n g e n c o u n t e r e d . A l t h o u g h s o m e of t h e s a m e species occur sporadically in the lower part of the CRP-3 section. the dominance of Not/1ofc/gidiie.s and Podocarpidifes species is less evident. Despite a low total Cenozoic miospore count of only 1 1 specimens.
t h e s a m p l e at 7 8 1 . 3 6 m b s f h a s a relatively h i g h taxonomic diversity with 9 species present.
Bryophytic spores 01' Co/~lo,Y/lor'il s p p . o c c u r corisisk~ntly tliroi~gli [lie seqiience (l-'igs. 3a. 311): most of these ;ire probably rel'e~~al>le to C o p ~ o x ~ o r u s11.c of Rai nc ( I WS). ;incl the C o p i o x p o i ~ ~ sp. I'roni CIROS- 1 illistrati~il by Mildenhall (IOSO. PI. 2. Fig. 14). T h e only oilier certain hryophytic spore encountered was a single broken specimen of I<ii~ci(icspoi~i/cs sp. similai- to thal seen in CRP-2A. which occurs :it 78 1.36 mbsf-.
Lycopod spores are noted Sor tlie first time in t h e sequence of C R P wells. as L y c o ~ ~ o d i i i ~ r ~ . s / ) o ~ ~ i t ~ . s sp..
and occur consistently through the upper part of CRP- 3. These differ from the exotic L y c o p c / i ~ ~ ~ i i spores (used as a tracer in preparations) i n having a finer- meshed reticulate sculpture and elevated membraneous a b r a ad,jacent to the laesurae. Ferns are represented b y rare o c c u r r e n c e s of C y ( ~ t h i d i t e s minor-.
L c ~ ( ~ ~ ' i ~ ~ t o s p o r i t e s spp. (Fig. 3c). and R~~gnlc~fi,s'/)orifes sp. It is possible that some of these fern spores are recycled from Eocene or older strata.
G y m n o s p e r m s are mainly represented b y Podoccirp/diies species. Pocloccirpidife.~ sp. a, which h a d a reported L A D at 3 16.50 mbsf i n C R P - 2 A ( C R S T . 1999, p . 1 3 6 ) . o c c u r s i n a few s a m p l e s . Podocar/;ic/ites sp. b and P.
cf.
e.x/g~~n'i (Fig. 3d) also occur in both CRP-212A and CRP-3. Poclocc17-/~ic/ites s p . d ( F i g s . 3e. 3 f ) is an u n c o m m o n form w i t h distinctive rugulate cappa. Poclocarpidites sp. e. a small form with clearly reticulate saccus mesexine (Figs. 3g, 3h), appears to have a peak in abundancebetween c. 7 1 and 13 1 mbsf. Dilu.\nifes g r a ~ i ~ ~ l c ~ t ~ ~ s , T r i c / i o f o ~ ~ ~ o s z ~ l c i f e ~ s subgraniilatus a n d
Microccichr\idites a n t a r c f i c u s (Fig. 3 i ) are, as i n CRP-212A comparatively rare and may be recycled f r o m older s t r a t a . A distinctive f o r m . c f . Trichoiomosulcites sp. (Figs. 3j. 3k). is not well- u n d e r s t o o d m o r p l ~ o l o g i c a l l y and may be a n undescribed species.
The diversity of Podocarpiclites species is possibly greater than is immediately apparent from table 1 . Taxonomic differentiation within the genus is difficult, a n d m a n y f o l d e d s p e c i m e n s have been r e c o r d e d simply as " P o d o c ( ; ~ p i d i f e s spp." A similar situation applies with A~ofliofagicliies. Nofhofagidifes asperus ( F i g . 4 g ) i s a distinctive l a r g e s p e c i e s w h i c h represents the me11:iesii pollen-morphological group.
Occasional specimens were also recorded in C R P - l and CRP-212A. With tlie exception of
N.
asperus, all specimens belong to the fusca pollen-morphological group. N. flemi17gii (Fig. 4f) is readily recognisable on t h e b a s i s of i t s relatively l a r g e size. m i n i m a l s c u l p t u r e . a n d p r o n o u n c e d apertural t h i c k e n i n g s ( c o s t a e ) . Atypically smaller specimens have been recorded as Al.cf.
flemir~gii. The distinction between more coarsely sculptured species of the fiisca group present in the C a p e Roberts cores requires further investigation. Specimens differing from typical N.lachlmiae (e.g. larger and with larger spines. Fig. 4e) have been recorded simply as Nothofagiclites spp.
@ / s e l l group).
Angiosperm pollen other than Nothofagiclites is granulate exine, Tricolpites sp. b (Fig. 3n) was seen uncommon. Two occurrences of possible Cyperaceae previously in the lower Oligocene section of CRP-2A pollen (?C\peraceaepo!!is sp.) complement a single at 453.26 mbsf. Other taxa occur as single specimens.
occurrence in CRP-2A (Askin & Raine, 2000, Fig.30. One (Figs. 31, 3m) is similar to Tricolpites sp. a seen Several species of dicotyledonous angiosperm pollen in the lower Miocene and upper Oligocene of CRP-1 are recorded as Tricolpites spp. An oblate form with and C R P - 2 / 2 A , but is s m a l l e r and has m o r e
Sample depth (m1 405 O M 0 6 07 405 5 9 4 0 8 G1 410 36-41038 i H 3 <!A13 13 424 52424 5-1 429 9 1 4 2 9 93 433 97 433 99 437 07A37 09 439 3 4 4 3 9 35 445 0 1 4 4 5 0 3 451 83-45? 83 457 3 7 4 5 7 39 W\ O l A 6 1 03 461 8 0 4 6 1 82 466 7 3 4 6 8 75 473 75.A73 77 474 73474 75 489 13-^G9 15 193 6 0 4 3 6 2 500 23-500 25 509 38-509 40 516 48-51550 52, 76-521 78 524 74-524 76 534 14-534 15 542 15-542 17 546 26-546 28 i 5 5 04-555 06 i 5 8 39-558 41 164 40-564 42
>B8 82 568 6 i i77 08-577 10 i81 35-581 37
$B4 44.584 46 i 9 i 81-591 93
$02 07-602 09
$05 2S-606 25 i17 60-617 62 i21 75.621 77 329 25-629 30 i33 20-633 22 i36 6 1 4 3 6 63 i40 69-640 71 843 6 0 4 4 3 62 848 23.646 25 i56 54-656 56 862 20-652 22 .79 8 1 4 7 9 8 3 88 9 6 6 5 8 S8 90 60-690 52 97 33-697 35 03 93-70395 07 55-707 57 20 10-720 20 22 58-722 55 31 28-73? 30 39 76-739 78 43 92-743 94 49 06-749 08 51 33-751 35 58 51-758 83 M 65-764 67 68 67-766 69 70 0 6 7 7 0 10 72 50-772 52 76 64-775 6s 77 7 0 777 72 81 10-781 12 81 24-781 26
." -
CONTEMPORANEOUS AND RECYCLED CEN0701C 11 IlRf STRIA1 PA! YNOMORI'HS
. . . .
S - ... - ... -
Spores and p o l l ~ n
. . .p.p.-. ... -- ... - ----I Recycled -P
pronounced polar exine thickening. Tricolpifes sp.d referred to Ranunculaceae (Figs. 4a, 4b): a similarly ( 1 0 7 . 3 8 mbsf, Fig. 30) and T r i c o l p i f e s s p . f sculptured but apparently alete pollen grain recorded ( 7 7 6 . 6 4 mbsf; F i g s . 3 p , 3q) a r e o t h e r f o r m s . A from CRP-2A was also ascribed to this family (Askin inicroechinate tricolpate pollen at 6 0 . 5 4 mbsf is & Raine, 2000. Fig. 31). A distorted but apparently
Fig. 3 - Photomicrographs of selected Cenoxoic spores and pollen from C R P - 3 . at uniform magnification (scale bar = 1 0 p m ) . a) Coptospoi.~~ sp.(= C o p m p o r o sp.c of Raine. 1998). depth 87.47-87.49 nihsf. slide P23213. England Finder coordinates T50(4). maximum dimension 45 ~111: 12) Coptospora sp.. 131.17-131 . l 9 mhsf. P22013. U38(3). 35 pm: c ) Lcie~igato.s1~0rites oviitu< Wilson & Webster. 114.90- 114.92 mbsf. P21612. X40(2j. 35 pm: d ) Podocurpidites c{. e.iigii~i.-i Harris. 114.90-1 14.92 mbsf. P21611. T50(4), breadth of corpus 25 inn:
e. 0 Poclocai~~if./ite.-i sp.cl. iwo focal levels. 107.38- 107.40 mhsf. P 18313B. G35(0). breadth of cot-pus 48 p111: g} Podocarpiditc", sp.e. 13 1.17- 1 3 1 . 1 9 m h s f . P22011. S 4 6 ( 3 j . l e n g t h 5 5 y m : h ) P o i l o r c i ~ ~ / ~ i d i t e . ~ s12.e. 1 1 4 . 9 0 - 1 1 4 . 9 2 m b s f . P21614. G 5 5 ( l ) . l e n g t h 51 p111:
i ) 1~4icrocc1cliryidite.s ant(~rcticiis Cookson. 92.28-92.30 n-ibsf. P23312. K50f4). 35 ~111: j , 12) cf. Tricliotoinosiilcite.~ sp.. two focal levels.
359.16-359.18 mbsf. P25711. K 5 3 ( 4 ) . 4 6 pm: I. m) 77icolpites sp.
(cf.
Tricolpites sp.a of Raine. 1998). two focal levels. 256.06-256.09 mbsf. P25311. B42(0). 33 urn: 1 1 ) Tricolpites sp.b of Askin & Raine (1998). 320.70-320.72 rnbsf. P27311. 043(2-4). 31 urn: ( 1 ) Trico1pile.s sp.d. 107.38-107.40 mbsf. P18312B. N22(1). 39 urn: p, q j 'Iricolpites sp.f, t\\o focal levels. 776.64-776.66 mhsf. P36412. D44(2). 21 pm:r) ?&Iyrtaceidite.s sp.. 2 10.7 1-2 10.73 mbsf. P24312. H 4 4 l ). 38 ~ i m .
Terrestrial Palynology of Cape Roher~s Project Drillhole CRP-3
Fig. 4 - Photomicrographs of selected pollen from CRP-3. at uniform niagnification (scale bar = 10 yrn) except for figure 11. Figures (1-1,
are thought to be Ceno~oic taxa penecontemporaneons with deposition. while specimens illustrated in figures S-II are redeposited from older Cenozoic or possibly Late Cretaceous strata, a. b ) Ran~~nculaceae. two focal levels, depth 60.54-60.56 mbsf. slide P22511. England Finder coordinates M39(0). niaximum dimension 37 urn: c, d ) PStylidiaceae. two focal levels. 195.62-195.64 mbsf. P23912. M38(4). 30 pm:
e) Notl~ofagidites sp. (fiisca group). 114.90-1 14.92 ~ n b s f . P21611. N45(0). 32 !.tm; f l A~ot17ofagidites fleniingii (Couper) Potonie. 114.90- 1 1 4 . 9 2 mbsf. P21611. S 3 4 ( 0 ) , 37 urn: g ) ~Vofho,fagidites a s p e r u s (Cookson) Romero. 82.36-82.38 mbsf. P18612. X35(2). 46 urn:
11) segregate of pollen of Notl~ofcigidites, lachlmioe (Couper) Pocknall & Mildenhall (scale bar = 10 pm). 101.59- 101.61 mbsf. P213/3, B45(0). individual pollen grains c. 27 p111 diameter: i, 1 ) Myricipites harrisii (Couper) Dutta & Sah, 781.36-781.38 mbsf. P34211 1. L47(2).
27 urn: k ) Triporopollenites sp.. 140.67-140.69 mbsf. P22213. V34(l). 53 ~ m ; l, 171) ?Campanulaceae. 87.47-87.49 mbsf. P23213. A48(0).
36 him: 11, o) ?Caryopliyllaceae. two focal levels. 127.88-127.90 mbsf. P21913. K34(0). 27 urn: p, a) Caryophyllaceae (Stella~.ia type). two f o c a l levels, 781.36-781.38 mbsf. P34217. S 4 6 ( 2 ) . 35 urn: r) C l ~ c ~ ~ o p o d i p o l l i s so., 265.41-265.43 mbsf. P25611. K50(0). 19 !.illl:
s) P e ~ ~ i ~ ~ s i ~ l ~ ~ p o l l i s
cf.
gill;; (Cookson) Dettmann & Jarzen. 177.76.177.78 nibsf. P23413. F38(3). 43 urn: t, 11) Trirolporites cf. p a e n e s t k t u s Stover. 83.02-83.04 mbsf. P20911, L33(2). 26 yni.i ~ l r a c o l p a t e pollen with n ~ i c r o e c h i n a t e sculpture recovered from 195.62 mbsf (Figs. 4c. 4d) may he referable to Stylidiaceae (there is also resemblance to R a n u n c ~ ~ l a c e a e ) . Possible Stylidiaceae pollen was r r e o r d e d from the lower Miocene section of ('RP-2/2A (Askin & Raine 2000. Fig. 2i). The present specimen appears to differ, for example in possessing larger echinae.
Four triporate pollen taxa are recorded. Myricipifes lieirrisii (Figs. 4i, 4j) is present only in the lower part 01' the CRP-3 section at 781.36 mbsf. A doubtful specimen also occurs at 4 7 4 . 7 3 mbsf. It has n o t previously been recorded in the Cape Roberts cores.
Pro/ec~cidites sp. (not illustrated) is a small form with gran~ilate exine. Triporopolle~~ite.~ sp. (Fig. 4k) is a large psilate form possibly conspecific with a specimen illustrated by Raine (1998, Fig. 2 d ) . A distinctive type recorded as PCampanulaceae occurs at 87.47 mbsf (Figs. 41, 4m). This species has scattered spines, thickened pore annuli, and protruding pore membranes, and may be conspecific with the species from CIROS-l recorded as PProteacidites spiniferns by Mildenhall (1989, PI. 2, Figs. 8-9).
T h r e e periporate pollen s p e c i e s , all possibly referable to C a r y o p h y l l a c e a e , a r e recorded a s Caryophyllaceae Stellaria type (only at 781.36 mbsf, Figs. 4p. 4q), PCaryophyllaceae (Figs 4n, 40): and C / ~ e ~ ; o ~ ~ o c l i p o l l i s sp. ( F i g , 4s). T h e latter two are similar to species occurring in CRP-l (CRST, 19980;
Raine, 1998, Figs. 2m & 2k-l respectively).
DISCUSSION
BIOSTRATIGRAPHY
M a r c h a n t i a c e a e and T~.icolpifes sp. a , t w o characteristic taxa of the uppermost Oligocene t o lower Miocene section of CRP-212A and tlie lower M i o c e n e section of C R P - 1 , a r e not recorded i n CRP-3. As noted above, the composition and relative abundances of taxa in the upper part of the CRP-3 sequence. down to c. 410 mbsf. resemble those of the lowermost Oligocene part of the CRP-2A section.
O t h e r than noting this consistency, the l a c k of established datunis at p r e s e n t precludes c l o s e r correlation. T h e apparent absence of the acme of Pocloca~pidifes sp. e in CRP-2, however, may suggest that the sequence between c. 71 and 131 mbsf in CRP-3 has no equivalent in CRP-2. in accord with other lines of evidence CCRST, 2000, p.187).
T h e diversity of C e n o z o i c taxa present in t h e upper part of the CRP-3 sequence is slightly less than that reported from CIROS-1 by Mildenhall (1989).
and less than in many of the middle to late Eocene
"McMurdo Sound erratics" ( M c l n t y r e & Wilson, 1966: Askin, 2000). A notable absence from CRP-3 is pollen of the brcissii group of Nofl~qf@gidites, present in the lower s e c t i o n of C I R O S - 1 . a n d in t h e
McMurdo erratics. If the CIROS- 1 occurrences c:in 1x3 regarded as contemporaneous with deposition. absciii.~i' o f the N. b r a s s i i g r o u p from CRP-3 p o i n t s t o ; I
younger age f o r the C R P - 3 s e q u e n c e : I I - ) H V G c. 410 mbsf. Again. this is consistent with r(*siills from marine biostratigraphy and ii~agnetosti'c~ii~i~iipliy i n CRP-3 (CRST, 2000; H a n n a h & Fielding rf : i l . ~ this volume) and the latest interpretations ol" ~ l i r ;I,".(,
of the fossiliferous CIROS-l strata ( H a n n a h ct al..
1997: Wilson et al.. 1998).
Below c. 4 1 0 mbsf in C R P - 3 (this d e p t h m:\\
correspond to the upper part of magnetochron ( ' l . % I ) .
i.e. about 3 3 . 2 M a and very early O l i ~ - > o c ~ i i ~ , according to Florindo et al., this volume). p;mcity of the assemblages and uncertainty about recycling and contamination prevent any conclusion being ilr;iwii with confidence. We note, however, that although rich 'warm-climate" preglacial Eocene assemblages were not encountered in CRP-3. there is some evidence i n support of such a correlation. Firstly, although only ;I
small number of miospores was recovered, spceii.~s diversity is apparently high in the 7 8 1 . 3 6 nihsl' sample. T h i s may suggest m o r e diverse parent vegetation. and therefore that a warmer cliniiitc prevailed. Second, the records of Myricipites /~(ii./~i,si/' at 781.36 and possibly 474.73 mbsf are t h e first record for the C R P sequence of wells. T h i s taxon.
which represents pollen of the angiosperm family Casuarinaceae. is characteristic and abundant i n the E o c e n e of New Z e a l a n d and Australia, a n d a l s o occurs in the McMurdo erratics (McIntyre & Wilson.
1966; Askin. 2 0 0 0 ) and M S S T S - 1 d r i l l core (Truswell, 1 9 8 6 ) . I n t h e M S S T S - 1 s e q u e n c e specimens are common through the upper Oligoccne.
lower Miocene, and Quaternary sections (Tr~iswcl l . 1986. r e c o r d e d as Triorites h a r r i s i i ) . a n d w e r e interpreted as recycled from older sediments. Rare specimens were recorded only in the lowermost part of the CIROS-1 sequence by Mildenllall ( 1 989. as Hc~lo~~agacidifes hcirri.s'ii), in the section now dated as middle Eocene, magnetochron C1 6n.2n (Wilson et al..
1998). In the glacial en-atics from McMurdo Sound dated as middle to upper Eocene on dinoflagellatc e v i d e n c e ( G r o u p 1 of A s k i n , 2 0 0 0 ) , M. h a r r i s i i (recorded as H. harrisii) occurs sparsely in only two samples. McIntyre & Wilson (1966) noted it as a minor component {T. hc/i~i.~ii) in three of five erratics samples studied.
In New Zealand, the main vegetational response to late E o c e n e climatic c o o l i n g o c c u r r e d s o m e time b e f o r e t h e e n d of t h e E o c e n e ( e . g . R a i n e , 1 9 8 4 ; Pocknall, 1989), near the K a i a t a n I R ~ ~ n a n g a n Stage boundary (35.5 M a , upper C16n: Morgans et al..
1996), a n d was reflected in tlie palynoflora by a t r a n s i t i o n f r o m M j r i c i p i t e s h u r r i s i i - d o m i n a t e d palynofloras to those dominated by Nothofagidites of the brassii group. It is likely that a corresponding vegetational change occurred at a similar time. or
even e a r l i e r . in ant arc tic;^. ' I ' l i i i t such ;I c1i;iiige o c c u r m l is attested to by the iibsc~ice o l ;l liirge propoi~tion of the rich Eocene I'loi-a, ;is noted ;ihove.
in the upper CRP-3 record. Whetlicr tlic speciiiiens of M. h(ir;~i,sii in CRP-3 ( a n d those i n GIROS- 1 ) :ire recycled is unclear. As noted, recycling o f 1\4. /idi'ri,sii would hi- unique within the known CI<P sequence. 11' the specimens are not recycleJ. then their presence may point to a Kaiatan-eqiiivalent or older age. i.e.
greater tlian 35.5 Ma, for these strata.
PALAl<Ol<NVIRONMENTAL SIGNIFICANCE It should be noted that cyclicity in sedimentary facies (Powell et al.. this volume) indicates there was significant fluctuation in glacial climate during the Oligoccne and lower Miocene CRP record. The spore- pollen assemblages do not provide a truly continuous record of vegetation. The palynological record must also have been smoothed by sedimentation processes such as peneco~itempora~ieo~is reworking. Further. the record emphasises the more favourable phases for plant growth, as periods unfavourable for vegetation will have provided less abundant spores and pollen to the sediments. Temperature estimates suggested here therefore apply to warmer phases during the relevant intervals.
Raine (1998) and Askin & Raine (2000) noted a close similarity of spore-pollen assemblages of the e a r l y M i o c e n e a n d l a t e O l i g o c e n e in C R P - l a n d CRP-212A to those of the Meyer Desert Formation of the Sirius Group in the Beardniore Glacier area of the Transantarctic Mountains (Askin & Markgraf, 1986), and inferred that they resulted from a similar tundra- like parent vegetation with sparse shrub Not11ofagu.s as well as a few other angiosperms. podocarps. and bryophytes. Comparison with present day climatic data for the Antarctic region (Longton, 1988) suggests that partial cover of low-diversity woody vegetation, b u t beyond t h e p o l e w a r d limit of e x t e n s i v e l y developed woodland would suggest mean January daily temperatures of at least 7'C but less tlian about 10°C* Polewards, vegetation beyond the limit of extensive s h r ~ ~ b l a n d but with important flowering plants and profuse bryophytes would imply mean January temperatures of at least 1-2OC but probably less than 7OC. Francis & Hill (1996) suggested from w o o d a n a t o m y t h a t t h e dwarf g r o w t h f o r m s of N o t h o f a g ~ ~ ~ s b e a r d m o r e n s i s in t h e M e y e r D e s e r t Formation may have grown in summer temperatures around S° or slightly higher. Mean summer daily temperatures of c. 5-7OC are accordingly proposed for t h e late O l i g o c e n e t o early M i o c e n e p e r i o d (c. 25-17 Ma) at Cape Roberts.
The Nothofagidites-dominated palynofloras of the lowerniost s e c t i o n of C R P - 2 a n d u p p e r C R P - 3 ,
correlated willi the early Oligocene. represent a more
1 x i ; i n t di-~vclo~)mcnt of woody vegetation. However.
<is noted tihove. a s s c m h l i ~ ~ c s i n tlie upper part of.
( ' R P - 3 never i'e;u'Ii (lie s p e c i e s richness a n d iihiinil;incc seen i n tlie l ~ o c m e McMurcIo S o u n d ermtics (Mclntyrc & Wilson, 1066; Askin. 2000) or in t h e I<ocene lower part of C I R O S - 1 (Mildenliall.
1989). Insteinl. the CI<ll-3 assenil>lages suggest low diversity woody v e g c ~ a t i o n that included several species of h/oth~f(~,i;tis ;iii(i podocarpaceoiis conifers. a few other angiosperm families. and few cryptogams except for hryopliytes (mosses and liverworts). Many of the important components of the prior Eocene flora a r e missing. I'or e x a m p l e several s p e c i e s ol' Proteaceae. various oilier angiosperms. gymnospernis a n d cryptogaiiis. I n favourable sites the vegetation may have comprised a low scrub or closed forest intermediate in stature and floristic richness between that of the Eocene a n d the limited vegetation of the l a t e O l i g o c e n e to early M i o c e n e . M o r e s t u n t e d vegetation would have existed in exposed and upland sites. Wctland vegetation, which would be indicated by the presence of i n o n o c o t y l e d o n o ~ ~ s angiosperms such as Cyperaceae and P l z o n n i ~ ~ m (CRP-2; CRST, 1999: Askin & Raine, 2000). appears to have been minor. although Copto,sporu may in part represent a mire community.
Phytolith a n a l y s e s ( T h o r n , this v o l u m e ) a l s o i n d i c a t e a p r o m i n e n t woody c o m p o n e n t to t h e vegetation during the period represented by the upper c. 410 ni of CRP-3 core. Smooth spherical phytoliths.
w h i c h a r e c o m m o n in t h e c o r e , a r e t y p i c a l o f Nothoj'c~gns s p p . , and o t h e r angiosperni t y p e s i n c l u d i n g possibly P r o t e a c e a e a r e a l s o p r e s e n t . Differing from the pollen record. Thorn suggests the p r e s e n c e of P a l m a e ( = A r e c a c e a e . p a l m s ) a n d G r a m i n e a e (= P o a c e a e , g r a s s e s ) . B o t h f a m i l i e s produce distinctive and reasonably abundant pollen.
but neither have been observed in the Cape Roberts pollen record, o r in t h e E o c e n e M c M u r d o S o u n d erratics. However Mildenhall (1989: 125) suggested s o m e records of Gramineae from CIROS-1 might represent in situ pollen.
Modern-day vegetation in the Magellanic Region at the southern tip of South America is put forward as a p o s s i b l e a n a l o g u e of t h e E a r l y O l i g o c e n e vegetation represented in the upper CRP-3 core. In this region at the southern limit of tree growth, low Nofiwfagus forests of very limited taxonomic diversity give way to stunted h ~ o t h o f a p s shrubland above the altitudinal treeline, only c. 650 m above sea level at Punta Arenas (McQueen. 1976). Climatic data for Punta Arenas (e.g. McQueen. 1976; Muller. 1982), w h i c h has a m e a n s u m m e r d a i l y t e m p e r a t u r e of
10.8OC. suggest a range of c. 10-12OC for the early Oligocene (c. 33-31 Ma) period at Cape Roberts.
T h e reader should note that temperatures quoted a s July (southern winter) monthly means i n Raine (1998) i n fact should have been quoted as January (southern summer) monthly means.
A C K N O W L E D G E M E N T S - W e i l i a n k J o h n S i m e s a n d T K A ( T e a c h e r s R x p e r i e n c i n ~ Aii~;irc[ii-';i) ;issistiini B r u c c S m i t h f o r t h e i r c a r e f u l p r e p a r a t o r y w o r k in t h e C r a r y . a b o r a t o r y , C R P m a r i n e p a l y n o l o g i s i s J o h n W r c n n am1 M i k e H a n n a h f o r c o m r a d e s h i p a t t h e m i c r o s c o p e . a n d V a n e s s a T h o r n f o r p h o t o g r a p h i c w o r k :it M c M u r d o . Reviewers A s h w o r t h , M a r k g r a f and Mildenhall are [hanked for t h e i r helpful c o m m e n t s . Supporf For tliis CRP r e s e a r c h for R a i n e w a s p r o v i d e d b y the N e w Z e a l a n d P u b l i c G o o d S c i e n c e F u n d , a n d f o r A s k i n by ( U n i t e d S l a t e s ) N a t i o n a l S c i e n c e Foundation grant OPP-9527013. I G N S Contribution Number 2220: B P R C Contribution N u m b e r 1227.
REFERENCES
Askin R.A.. 2000. Spores and pollen from the McMurdo Sound crratics. Antarctica. In: Stilwcll J . D , & Fcklmann R.M. (eels,).
P a l a r o l ~ i o l q y and P a l a e o ~ i ~ ~ ~ i r o i ~ i ~ u ' n i ' : o,f Eocene R o c k s , McMii~.c/o Sound. East Antarctica. Antarctic Research Series.
76. American Geophysical Union. pp. 16 1-1 8 1.
Askin R.A. & Markgraf V.. 1986. Palynomorphs from the Sirius Formation. Dominion Range. Antarctica. Aiiforcfic Journal of
the United States. 21. 34-35.
Askin R.A. & Raine J.I.. 2000. Oligocene and Early Miocene terrestrial palynology of Cape Robcrts Drillhole CRP-212A.
Victoria Land Basin. Antarctica. Terra Ai~torfica. 7. 493-501.
Cantrill D . , 2 0 0 1 . Early Oligocene N o t h q f a g i i s from C R P - 3 . Antarctica: in~plications for the vegetation history. This volume.
Cape Roberts Science Team. 1998a. Background to CRP-1. Cape Roberts Project. Antarctica. Terrc; Ani(~rticd. 5. 1-30.
Cape Roberts Science Team. 1998b. Miocene Strata in C R P - I . Cape Roberts Project. Antarctica. Terra Antartico. 5. 63-124.
Cape Roberts Science Team. 1998c. Summary of results from CRP- 1. Cape Roberts Project. Antarctica. T e r m Antartica. 5. 125- 137.
Cape Roberts Science Team. 1999. Initial Report on CRP-212A.
Terra Antartica. 6. 1-173.
Cape Roberts Science Team. 2000. Studies from Cape Roberts Project. Initial Report on CRP-3. Term Antartica. 7. 1-209.
Dcttmann M.E. & Jarzen D.M.. 1988. Angiosperm pollen from uppermost Cretaceous strata of southeastern Australia and the Antarctic Peninsula. Memoir of the Association of Australasian Palaeontologists. 5, 217-237.
Florindo F.. Wilson G.S.. Roberts A.P.. Sagnotti L. & Verosub K.L..
2001. Magnetostratigraphy of late Eocene - early Oligocene glaciomarine sediments from the CRP-3 core. Victoria Land Basin. Antarctica. This volume.
Francis J.E. & Hill R . S . , 1996. Fossil plants from the Pliocene Sirius Group, Trasisantarctic Mountains: evidence for climate from growth rings and fossil leaves. Palaios, 11. 389-396.
Hannah M.J.. Cita M.B.. Coccioni R. & Monechi S.. 1997. The EoceneIOligocesie boundary at 70Â South. McMurdo Sound.
Antarctica. Terra Antartica. 4 , 79-97.
Hannah M . J . . F i e l d i n g C . , Florindo F. & Harwood D . . 2 0 0 1 . Chronostratigraphy of CRP-3. Victoria Land Basin. Antarctica.
This volun~e.
Hannah M.J.. Wrenn J.H. & Wilson G.J. 2001. Early Oligocene
111ari11e piiIynomorpli.s from GRIP-3. Victoria Lain1 iiitsin.
A~iliircticii. This volume.
Kcmp l';.M. & llairis \V.K,. 1977. The piilyuology of early '1'rrli;iiy scdimcnts. Ninctyciist l<i(lgc. linlian Ocean. Special /iii/ii'r\ in
~ i i / t i ~ ' O i i ~ i ~ / O , ~ l ~ , $ 0 . 70 p.
Len$toii R.l;.. 1988. 'I'lic I~iiilo,q~ o f polc~r br\oph\n"i c i n ( 1 licliriii.
Cambridge University Press. Cambridge.
Macphiiil M . S . 1990. Palyiiostriitig~-apliy of the M u m i y 13iisi11, inland southcastcrn I\IIS~I-iilia. I ~ i i o l o g ~ 23. 197-240.
Mclntyrc D..I. & Wilson (;..l.. 1966. Preliminary palyniilo;!y ot some Antarctic Tcrliary erratics. ~Vcir Zealand Joiii'niil I > /
Botciny. 4. 3 15-32 1 .
McQuccn D.R.. 1976. 'I'hc c c o l o g ~ o f Aroll~(;f(~,g~~s and iissocialril vegetation in South Aincric;~. Tuiifura, 22. 38-68.
Mildenliall D.C.. 1989. Tci~cstriiil palynology. In: Barrett I1..l. (ril.).
A n t c i ~ ~ ~ t i c C c u o ; o i c !n.\!oi.~ from the C I R O S - 1 d r i l l h o l e , McMurdo Sound. DSIR Bulletin. 245. 119-127.
Morgans H.E.G.. Scott (3.1-1.. Ben A.G., Graham I.J.. Mnniiiic '1'.
C.. St Gcorze W. & Strong C.P.. 1996. New Zealand Ci.-ilo/oic time s c a l e ( 1 9 9 6 ) . l i ~ , s t / t i t i e o,f G e o l o g i c a l ancl Niifli'iir Sciei~ce,~, Science R O I I O I . ~ . 96/38.
Muller M . J . . 1982. S e l e c t e d c l i m a t e d a t a f o r a g l o l x i l ,S<-/ 111
,stiindard stations , f i r i'~y(,/ation science. W Junk. Tin- l lapin', 306 p.
Pocknall D. T.. 1989. Late Eocene to Early Miocene vegetation i i n i l
climate history of New Zealand. Journal of the Royal .Siici(~f)~
of New Zealand. 19, 1- 18.
Pocknall D.T. & Mildenhall D.C.. 1984. Late Oligoccnc-carly Miocene spores and pollen from Southland. New Zealand. /\/cir Zealand Geological S i i r v q Palaeontologicc~l Bulletin. 51. 06 p.
Powell R.D.. Fielding C.R,, Laird M.G.. Naish T.R.. van tlcr Mccr J.. 2001. Depositional environments for strata cored by CRP-3.
Victoria Land Basin. Antarctica: p a l a e o g l a c i o l o g i c a l and palaeoclimatic inference-). This volume.
Raine J.I.. 1984. Outline of a palynological zonation of Cretaceous to Palaeogene terrestrial sediments in West C o a s t Rcgion.
South Island. New Zealand. iVeir Zealand Geological .S'HI-I'CJ Report ATZGS. 109. 82 p.
Raine J.I.. 1998. Terrestrial palynomorphs from C a p e Roberts Project drillhole CRP-l. Ross Sea. Antarctica. T e r m Anicirticd.
5. 539-548.
Raine J.I. & Tremain R . , 1992. Apparatus for rapid sieving of palynological residues, New Zealand Geological Survey repoi't PAL, 151. 14 p.
Simes J. & Wrenn J.H.. 1998. Palynologic Processing in Antarctica.
Terra Antartica. 5. 549-552.
Stover L.E. & Partridge A.D.. 1973. Tertiary and Late Cretaceous spores and pollen from the Gippsland Basin. southeastern Australia. P r o r e e d i ~ ~ g s o,f the Royal Society of Victoria. 85.
237-286.
Thorn V.. 2001. Oligocene and Early Miocene Phytoliths from CRP-212A and CRP-3. Victoria Land Basin. Antarctica. This volume.
Truswell E.M.. 1986. Palynology. In: Barrett P.J. (ed.). Antarctic C e n o z o i c history from the MSSTS-1 drillhole. McMui-clo Sound. DSIR Bulletir~. 237, 13 1 - 134.
Wilson G.S.. Roberts A.P.. Verosub K.L.. Florindo F. & Sagnotti I...
1998. Magnetobiostratigraphic chronology of t h e Eocenc- O l i g o c e n e transition in the C I R O S - l c o r e . Victoria Land margin. Antarctica: implications for Antarctic glacial history.
Geological Society of America bulletin. 110. 35-47.
