IliA

Journal oJ NannopJankton
Research

6TH INTERNATIONAL NANNOPLANKTON ASSOCIATIONCONFERENCE
CoPENHAGEN 1995
PROGRAMME AND ABSTRACTS

A Publication of the International Nannoplankton Association
Volume 17

Number 2

ISSN 1210-8049

1995

JOURNAL OF NANNOPLANKTON RESEARCH(formerly INA Newsletter)
Published by the International Nannoplankton Association
Volume17

Number2

January 1996

ABSTRACTS ............ ............................................................................................... ... ........... .. .. .............................................................. 46

NEOSPHAERA COCCOUTHOMORPHA AND CERATOIJTHUS CRISTATUS:
ARE THEY THE SAME SPECIES ? J. Alcober and R. W Jordan .................................................. .......................... .... ......... 46
NANNOFOSSILS OF THE MAASTRICHTIAN-PALEOCENE GERMAV FORMATION,
SOUTHEAST ANATOLIA, TURKEY
Seving Ozkan and D. Altiner .......................................................... ............ .. ........ 46
CALCAREOUS NANNOFOSSILS FROM CAL VELLO BASIN (SOUTHERN APENNINES, ITALY)
Filomena Ornella A more ............................................................................................................. ........... ............................ .............. 46
PRODUCTION, SEDIMENTATION AND PRESERVATION OF COCCOLITHOPHORESIN THE NORTHERN NORTH ATLANTIC
Harald Andruleit ........... ................................ .......................... .. ..................... 47
THE TURNOVER OF CALCAREOUS PHYTOPLANKTON FROM THE BARREMIAN-APTIAN
BOUNDARY INTERVAL IN NW EUROPE
Gregor Bischo.ff and Jorg Mutterlose ................... ................. ............. ........ 48
JURASSIC-EARL Y CRETACEOUS CALCAREOUS NANNOFOSSILS FROM
THE NEUQuEN BASIN, ARGENTINA
P.R. Bown and C. Ellison ........................... ........ ................. ................................ 48
COCCOLITH BUILDING BLOCKS: HIGH RESOLUTION ANALYSES OF
HETEROCOCCOLITH MORPHOLOGY AND CRYSTALLOGRAPHY
P.R. Bown, J.R. Young, T.E. Ehrendorfer, S.A . Davies, J.M. Didymus and S. M ann ............................................................ .48
ALBIAN/CENOMANIAN TO KIT STAGE BOUNDARIES AND NANNOFOSSIL EVENTS:
INCREASED PRECISION IN UPPER CRETACEOUS NANNOFOSSIL BIOSTRATIGRAPHY
AND CORRELATION Jackie Burnett ..................................................... ........... ... .. .. .. .. ... ....... ............. ................................... . 49
SOME CALCAREOUS NANNOFOSSILS MISINTERPRETED IN LITERATURE AS TETRAIJTHUS,
TRIQUETRORHABDULUS, FUSEU/NUS SP. ARE ACTUALLY SPICULES OF DIDEMNUM SSP.
(TUNICA TA, ASCIDIAN). EVIDENCE FROM UPPER JURASSIC SEDIMENTS OF CHARENTES(YV. FRANCE)
Georges Busson, Denise Noel, Fram;oise Monniot and Annie Cornee ..................................................... 49

COCCOIJTHUS PELAGICUS, A SORT OF PRODUCTMTY PROXY ?
Mario Cachiio and M. T. Moita .................................... .................................. ............................. .............. ........ ............................... 50
AN EXAMINATION OF THE GLOBAL RELATIONSHIP BETWEEN THE LAST TWO "SPECIES" OF
A /ex Chepstow-Lusty and Mark Chapman .................................. 51
DISCOASTERS AT THE END OF THE PLIOCENE
COCCOLITHOPHORID DISTRIBUTION ACROSS A TRANSECT BETWEEN THE IBERIANPENINSULA AND THE BALEARIC ISLANDS (NORTHWESTERN MEDITERRANEAN SEA)
Lluisa Cros ... ............ ... ......................................... ............................ .................... .................... ......... ........................................... ..... 53
CALCAREOUS PLANKTON BIOSTRATIGRAPHY AND 40AR/39AR DATING OF VOLCANIC
ASH LAYERS FROM MONFERRATO (NW ITALY)
A. d'Atri, A. Novaretti, R. Ruffini, MA. Cosca and J.C. Hunziker ............................................................................................ 53
PALEOCENE TO EARLY EOCENE CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY
Eric de Kaenel ........................ ............................................................................... 54
OF THE EL KEF SECTION (TUNISIA)CALCAREOUS NANNOFOSSILS BIOSTRATGRAPHY OF THE PLIO-PLEISTOCENE
Agata di Stefano ............... .......... .... ............................. 54
DEPOSISTS OF THE PELORITANI MOUNTAINS (NE SICILY)
PALEOECOLOGY OF THE PALEOCENE NANNOPLANKTON
0/ga B. Dmitrenko .......... .......................... ......... .. ....................... .......................... .......................................................... ................... 55
CALCAREOUS NANNOFOSSILS AS PALEOPRODUCTIVITY INDICATORS IN CAMPANIANYoram Eshet and Ahuva Almogi-Labin ................................................ 55
MAASTRICHTIAN UPWELLING SYSTEMS

41

CALCAREOUS NANNOFOSSIL DATUM LEVELS : A KEY FOR THE UNDERSTANDING OF THE
GENESIS OF UPPER CRETACEOUS OIL SHALE SECTIONS IN ISRAEL
Eshet, Y., Minster, T., Moshkovitz, S. ...... .. .... ........... ... ...... ................. .. .. ..... ... ... .... .... .... ... .. ......................... .. ....... ... .. .. .... ..... ......... 56
CALCAREOUS NANNOFOSSIL BIOSTRA TIGRAPHY IN SANTONIAN-MAASTRICHTIANORGANIC-RICH CARBONATE SECTIONS IN ISRAEL
Y. Eshet, and S. Moshkovitz ... ...................... ............. .. ..... ... 56
CALCAREOUS NANNOPLANKTON FROM THE AUSTRALIAN SECTOR OF THE SOUTHERN OCEAN
C/aire Find/ay ................... ........ ... .... ........ .. .... .. ............. ...... .. ........ .. ................. .. ...... .. ....... ... .. .... .. ............... .............. .... ............. ... ... 57
MAASTRICHTIAN NANNOFOSSIL BIOGEOGRAPHY IN THE SOUTHERN TETHYS
Andrea Fiorentino ................................... ................... .......................... ........... ............. .. ..:................................................... ........... 57
AN EXAMPLE OF EUTROPHIC-OLIGOTROPHIC ALTERNATES IN THE LOWER MESSINIAN:
THE SORBAS BASIN (WESTERN MEDITERRANEAN)
J.A. Flares, FJ. Sierra, I. Zamarreno, A. Vazquez, R. Utrilla and G. Frances .. ... ................................ ........ ......................... 58
BIOSTRATIGRAPHY USING SILICOFLAGELLATES AND CALCAREOUS NANNOFOSSILS
Patras Dimitris Frydas ........... .. ... .. ............... .. ..................... 58
OF NEOGENE-PLEISTOCENE DEPOSITS OF GREECEEARLY CRETACEOUS CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF THE INTERNAL
LIGURIDS (NORTHERN APENNINES, ITALY) AND THE ONSET OF COCCOLITH-BEARING
SEDIMENTS IN THE LIGURIAN-PIEDMONT OCEANIC DOMAIN
Si/via Gardin and Nicola Perilli ........ .... .... 59
SEDIMENT TRAP STUDIES OF COCCOLITH AND PLANKTONIC FORAMINIFERAL FLUXESIN THE BENGUELA UPWELLING SYSTEM
Jacques Giraudeau and Geoffrey W Bailey .... ..... .. ........ .............. ..... 61
OCEANIC FRONTS IN THE MESOZOIC
William W Hay ......................... ............... .. ... .. .. ... .. ...... ...... ... ....... .. .. .... .................. ... .. .. .... .. ............ ... ........ ...... ........ .. .. ..... ........ .. .. .. 61
CALCDINOCYSTS FROM THE MIDDLE CONIACIAN TO UPPER SANTONIAN CHALKSAT LAEGERDORF (N GERMANY)
Tania Hildebrand-Habel and Helmuth Willems ............. .. ................. ....... .. ... ..... 62
UPWELLING RELATED Dil'{OFLAGELLATE CYST ASSOCIATIONS OF THE BENGUELACURRENT SYSTEM
Ramses P. Hoek and Karin A.F Zonneveld ........................ ......................... ................................ .. 62
CORRELATION OF CALCAREOUS AND ORGANIC-WALLED DINOFLAGELLATE CYST ASSOCIATIONSIN GLACIAL/INTERGLACIAL CYCLES, AN EXAMPLE OF THE EQUATORIAL ATLANTIC
Christine Hoe// ........................ ............. .. .. ......... ... .. .... ........ ...... ... ..... .. ........... .. ... ............... .. ... ..... .................. .. ......... ........................ 63
MID-CRETACEOUS CALCAREOUS NANNOPLANKTON IN AN ORGANIC-RICH FACIES OF
THE SUBBETIC AND PENIBETIC (BETIC CORDILLERA, SOUTHERN SPAIN)
Glen Homeier ............................ 63
MID-LATE CRETACEOUS NANNOFOSSIL BIOSTRATIGRAPHY OF THE PAPUAN BASIN,PAPUA, NEW GUINEA
Richard Howe ................ ........................................ .. .......... ...................... .. .... ............................... 64
BIOSTRATIGRAPHY IN THE OIL INDUSTRY
Martin Jakobowski ......... .. ...................... ............... ............. ............. ............ ................. ................ ................. .... .... .................... ...... 64
CALCAREOUS DINOFLAGELLATE CYSTS: ULTRASTRUCTURE TYPES AND SYSTEMATIC
Dorothea Janofske, Helmut Keupp and Helmut Willems .................................... ............ ................ ..... 64
APPLICATIONCOMPARATIVE VARIATION OF CALCAREOUS NANNOFOSSILS(ESPECIALLY ELLIPSAGELOSPHAERACEAE), FORAMINIFERS AND ORGANIC MA TIER
CONCENTRATION IN THE KIMMERIDGIAN SEQUENCE FROM LA BR.l:ERE (NORMANDY, FRANCE)Marie-Christine Janin, Yann Samson,, M aria Saint-Germes, Franryois Baudin and Gerard Bignot ........... ....................... 65
THE CASE OF THE MISSING NANNOFOSSIL OR "NOW YQU SEE IT, NOW YOU DON' T"
David Jutson ........... ......................................................... ................ ........................ ........................ ................ ......................... ....... 66
LATE PLIOCENE NANNOFOSSIL BIOEVENTS AND THEIR BIOSTRATIGRAPHIC ANDPALEOCEANOGRAPHIC MEANINGS
Koji Kameo, Tokiyuki Sato, and Toshiaki Takayama .................... ............. 66
CALCAREOUS DINOFLAGELLATES OF THE EQUATORIAL ATLANTIC OCEAN
Beate Kemtopf. ................ ............................................................................... :............... ............ ................. .......... ... .. .......... ............ 67
CALCAREOUS DINOFLAGELLATE CYSTS OF THE LATE ALBIAN AND THEIR ENVIRONMENTALDEI)UCTIONS (BOREHOLE KIRCHRODE 1/91 , GERMANY)
Helmut Keupp ................................................... .......... 68

42===========================

DEVELOPMENT OF CALCAREOUS DINOFLAGELLATE CYSTS (CALCIODINELLACEAE
DEFLANDRE, 1947) AT THE CRETACEOUS-TERTIARY BOUNDARY (NE GERMANY, DENMARK)
Ulrike Kienel ................................... .. .... ...................... ..... ............................ .. ..................................... .. ............ ................................ 68
A 300 KYRS CALCAREOUS PLANKTON RECORD OF THE EQUATORIAL SOUTH ATLANTIC:RECONSTRUCTIONS OF SURFACE WATER PRODUCTIVITY AND BOTTOM WATER DISSOLUTIONCYCLES
H. Kinkel, N. Ditert, K.H. Baumann ........................................................................................................................ 69
THE MIOCENE BLUE CLAY FORMATION OF THE MALTESE ISLANDS: SEQUENCE-STRATIGRAPIITC
AND PALEOCEANOGRAPIITC IMPLICATIONS BASED ON CALCAREOUS NANNOFOSSIL
STRATIGRAPHY AND CALCAREOUS DINOFLAGELLATE CYSTS
U. Kienel, U. Rehfeld, S. Bel/as and R. Kohring .... ............... .. ............ ..................... .............................................. .. ............ ....... 69
CALCAREOUS NANNOPLANKTON RESPONSE TO TERMINATION II AND HEINRICH EVENT(140-110 KA BP) IN THE NE ATLANTIC Anna Lotoskaya and Patrizia Ziveri .......................... .. ............. .. .................. 70
CALCAREOUS NANNOPLANKTON BIOSTRATIGRAPHIC ANALYSIS AS A TOOL FOR THE
STUDY OF DISCONTINUITY SURFACES IN THE CRETACEOUS OF THE TRENTO PLATEAU(SOUTHERN ALPINE, !TALY)Francesca Lazar ....... ....................................................... ................................ ............... ... 71\

PLEISTOCENE CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF SITE 577 LEG 86, NORTHWESTERN PACIFIC OCEAN
Patrizia Maiorano, Maria Marino and Simonetta Monechi .......................................... 71
CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF EARLY-MIDDLE PLEISTOCENEMaria Marino ........ .. .. .. .. .. .......... ............ ... ...... ........... .................. 72
TERRIGENOUS SEDIMENTS (SOUTHERN ITALY)CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF THE LATE CRETACEOUS-EARLY TERTIARY
OF WADI FEIRAN AND GEBEL QABELIAT, SOUTH WESTERN SINAI, EGYPT· Akhmal M Marzouk and Mohamed K. Abou-EI-Enein ........ ........................... ................................. ........... ...... ........................ 73
CALCAREOUS NANNOFOSSILS BIOSTRATIGRAPHY OF THE FUENTELSAZ (SPAIN)
AND FillMINATA (ITALY) SECTIONS: LATE TOARCIAN-EARLY AALENIAN
Emanuela Mattioli and Nicola Perilli ......................................... ........... .. ...................................................................................... 73
CALCAREOUS NANNOFOSSIL ASSEMBLAGES IN THE CENOMANIAN AND TURONIANDEPOSITS IN LITHUANIA
Romualda Mertiniene .................... .. .. ............................................... ....................................... 74
NANNOPLANKTON ZONES IN THE VOLCANIC TUFFS OF THE TRANSYL VANIAN BASIN (MIOCENE)
Nicolae Meszaros .. ..... ..... ................................................................................ ................... .. .............. ........... ................................. ... 75
lllGH RESOLUTION BIOSTRATIGRAPHY OF THE AMAZON FAN
Naja Mikkelsen .. ............ ............................................ ......... ....................................................... .. .. .................................. .. .. .. .. .......... 76
A STUDY OF THE FORAMINIFERAL AND CALCAREOUS NANNOPLANKTON ASSEMBLAGES OF
CORE SAMPLES TAKEN FROM THE LAHAR-AFFECTED PORTIONS OF THE SOUTH CHINA SEA
IN ZAMBALES PROVINCE, PHILIPPINES
Priscilla J. Militante-Matias and Marietta M De Leon .......................... 76
CALCAREOUS NANNOFOSSII-S (HAUTERIVIAN) FROM "AGUA DE LA MULA" SECTION,
NEUQuEN PROVINCE, ARGENTINA
E. Mostajo, A. Concheyro, F D. Zquez .. ........................................................... 76
CALCAREOUS NANNOFOSSIL PALEOCEANOGRAPHY OF THE LOWER CRETACEOUS OFNORTHWEST EUROPE
Jorg Mutterlose ................................................................................................ .. ... ......................... 77
THE NANNOPLANKTON OF THE JASLO LIMESTONE HORIZONSAndras Nagymarosy ............................................................................................................................................................ ............. 77
CALCAREOUS NANNOPLANKTON BIOSTRATIGRAPHY OF THE SALZGITTER-SALDERLIMESTONE QUARRY, LOWER SAXONY, GERMANY
F Naji ............................................... ...................................... 78
FLORISTIC AND ISOTOPIC CHANGES AT THE PALEOCENE-EOCENE BOUNDARY IN SLOVENIA
Jemej Pavsic and Tadej Dolenec ..... ....... ............................................................ ................................... ....................................... 79
MORPHOMETRIC AND BIOCHRONOLOGIC STUDY OF COCCOUTHUS MIOPEIAGICUS
Alyssa Peleo-Aiampay .............. ......................................................................................................................................................... 80
CALCAREOUS NANNOFOSSILS, TSUNAMITES AND THE Kff BOUNDARY OFNORTHEASTERN MEXICOJames J Pospichal ........................................................................................ .......................... 80
CALCAREOUS NANNOFOSSILS AND PALYNOMORPHS FROM VALANGINIAN AND
HAUTERIVIAN (LOWER CRETACEOUS) STRATA OF CERRO DE LA PARVA, CENTRAL-WESTERN
NEUQuEN, ARGENTINA
M Pramparo, W Volkheimer, and E. Mostajo .......................................................... .......... 81=========================43

PALEOECOLOOY OF CALCAREOUS NANNOFOSSIL ASSEMBLAGES AND ITS RELATIONSHIPTO SEA-LEVEL VARIATIONS IN THE FIGOLS GROUP (EARLY EOCENE, SPANISH PYRENEES)
Viviana Rea le.. ... .. ...................................... .. ................................................. .. ......................................... .................................... .. ... 81
CALCAREOUS NANNOPLANKTON FROM THE BOUNDARY DEPOSITS OF MAASTRICHTIAN
Anna Romaniv ................................................ ..... ................... 82
AND DANIAN OF THE UKRAINIAN CARPATHIANSNANNOFOSSILS AND PLANKTIC FORAMINIFERA ACROSS THE K/T BOUNDARY IN TWOSECTIONS OF NORTHEASTERN MEXICO

a::;:i::I:;:-:::;:~S:i::t~a=:~::~ ;;::E:;~:-::~::~~-~· · ·························REFERE~CE

83

THE JAPAN SEA SIDE, WITH
TO THE GLACIATION IN THE ARCTIC SEATokiyuki Sato and Koji Kameo ............... .. ..................................................................................................................... ............... 83
LATE CRETACEOUS BIOSTRATIGRAPHY AND PALEOCEANOORAPHY OF THE ATLANTIC
COASTAL PLAINS, USA
Jean Self-Trail .................................... .................................... .. ................................................... 83
PALEOOENE AND NEOOENE PRODUCTMTY IN THE INDIAN OCEAN
William G. Siesser ........... .. .. ........ ............. ......... ........ ... .. ........... .. .......................................... .. ..................... .. ........... ....................... 84
DEVELOPMENT OFITHE PLIO-PLEISTOCENE COCCOLITH ASSEMBLAGES IN THE NE
ATLANTIC CORREI.jATED TO CLIMATIC CHANGESXin Su ............................................... ........... .............. ........... 84
RARE OCCURRENCES OF PETRARHABDUS COPULATUS DEFLANDRE ON THE NORTHERNHEMISPHERE (CENTRAL EUROPE)
Lilian Svtibenickti ..................... ....... .. ........... ..... .............. .. .. ...... .......... ............... .. 85
THE DANIAN (LOWER PALEOCENE) LIMESTONE DEPOSITS IN DENMARK: BASIN
Erik Thomsen ....... ............ ............................... ... ... ................. 86
DEVELOPMENT AND SEQUENCE STRATIGRAPHY
POLAR COCCOLITHOPHORIDS
Helge Abildhauge Thomsen ....... .. ................................. .. ...... .. ............................ ................ ................................................ .. ...... .... 87
CHANGES OF CALCAREOUS NANNOPLANKTON EVOLUTIONARY DIVERSITY DURING
THE PALEOOENE
Maola Ushakova ..................................... ...................... .. .. .. .................................................................. 88
UTILITY OF CALCAREOUS NANNOFOSSILS AND ORGANIC REMAINS: IN THE RECONSTRUCTION
OF THERMAL METAMORPillSM IN THE HATRURIM FORMATION (TERTIARY, SOUTHERN ISRAEL)
S. Volin, Y. Eshet, and H. Kish .................................................................................. .. .............................. .. .............. ................ .. .. 88
CALCAREOUS NANNOFOSSILS IN THE ARTS
Katharina von Sa/is .................. .. .......... .. .................. ........... .................. .......... .. ........................................ .... ....................... .. .. ...... 88
NANNO NOTES: AN INTERACTIVE DIGITAL IMAGE CATALOG OF CENOZOIC CALCAREOUS
NANNOFOSSILS
Sherwood W. Wise, Jr., Linda Tway, Darren D. Milman, Wi/liam C. Payton, James J. Pospichal,
Jay Muza, Patrizia Maiorano, Andrea Concheyro, Giuliana Villa, Katharina Perch-Nielsen,
Laurel M . Bybell, Jean M . Self-Trail, William L. Murphy, Wi/liam R. Riede/, and Yan Xu ............ .. ................................... 90
THE INITIATION OF NORTH ATLANTIC DEEP WATER AS DATED BY NANNOFOSSILS
Wuchang Wei ............................ .. ... ..................................... ....................... .................. .. .. ........... ........................................ .............. 90
CALCAREOUS DINOFLAGELLATE CYSTS AT THE KIT BOUNDARY OF THE GEULHEMMERBERG(LIMBURG, THE NETHERLANDS)
Helmut Willems ....................................................... .............. ................................. 91
LIVING COCCOLITHOPHORID ASSEMBLAGES OFF THE PUERTO RICAN SHELF
A. Winter and R.W. Jordan ............................................................. ............ .. ..................... .. ..................... ............. .. .......... ...... ..... 91
NON-CONVENTIONAL' NANNOPLANKTON BIOSTRATIGRAPHY APPLIED TO BIOSTEERING
HORIZONTAL WELLSCharles R. Young ......................... ................... ...................................... ...... ................................... 92
COCCOBIOM - A LIGHT MICROSCOPE BASED IMAGE CAPTURE AND MORPHOMETRICS
APPLICATION FOR EMIUANIA HUXLEYI AND OTHER COCCOLITHS
Jeremy R. Young, Jackie A. Burnett, and Michal Kucera ............ ................................... ..................... ..................................... 92
STUDIES OF COCCOLITHOPHORIDS FROM THE ARABIAN SEA AND THE NORTH INDIAN OCEAN
Alexandra Zeltner .................... ....... ........... .. ................................................. .............. .................. .. ........ .. .. .. ...................... ......... .. ... 94
PARTICIPANTS ... ... .. ...................................... .. .. ... .. .......................... .... ...... ........... ........ .. ............................ .................... ........... ..... .... 95
PROGRAMME ... ............................. ....... .. ......................... .. ... .. ........... .. ................................ .......... ..... ........................................... .. .... 98
POSTERS ... ................................. ............ .............. ............................ .. .. ........ .. .......... ..... ... .................................................................... 100

44=============================

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

EDITORIAL NOTE

The 6th International Nannoplankton Association
conference was held in Copenhagen from September 3 toSeptember 6, 1995. More than 80 participants from 22 countries presented 29 talks and about 40 posters. The abstracts of all contributions were presented in an Abstract
Volume, edited by Niels. E. POULSEN which was given to
all conference attendants. But we felt that also the other
INA members, who were not able to come to Copenhagen,might be interested in topics that had been discussed there.
With the permission of the organizing committee,
this special JNR number brings the re-edition of the abstracts. We did not make any changes in the text, except a

45

few autograph corrections, so a couple of abstracts for thecontributions that were not actually presented at the conference are included. The only change we made concerns
the headings fonts etc. according the JNR custom.
In this place, we would like to express our thanks to
the Organizing Committee, namely to David JUTSON,
Hanne S0RENSEN and Niels. E . POULSEN for their collaboration during preparation of this volume and theirenormous organizing work and to the DGU for the permission to publish the abstracts in the Journal of Nannoplankton Research.

Editors

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

ABSTRACTS
NEOSPHAERA COCCOLITHOMORPHA AND CERATOLITHUS CRISTATUS :ARE THEY THE SAME SPECIES?
J. Alcober and R. W Jordan
Poster session
In current classification schemes there are almost 200 speciesof living coccolithophorids, however, only a few of theirlife cycles are known. 'This is largely due to the difficulties
of establishing them in unialgal cultures. At present, maybe
only 10 species have been successfully isolated andmaintained, and of these most are either coastal or common
oceanic taxa. Another problem lies in their relative
inaccessibility. Many coccolithophorids live in subtropicalwaters, away from the continental shelf, and so an oceangoing research vessel is often needed. Common on-board
collecting methods normally involve filtrations orpreservation, as single cell isolation is extremely difficult toperform at sea, -and maintaining wild populations normallyselects the ' weeds'. Therefore, there is a need to document
obsenrations made from filtered or preserved material, andrecently, a number of potential life cycles have beenreported in this way. However, these findings will needverification from culture observations when cultures
become available.

In this presentation we show a possible relationshipbetween two well known type species, Neosphaera
cocco/ithomorpha and Ceratolithus cristatus. In the
coccolithophorid life cycles reported so far, one phaseemerges from inside the other, causing the displacement of
the older phase coccoliths. In one of our specimens of N
coccolithomorpha an emerging C. crista/us coccosphere,
composed of hoop-like coccoliths, can be seen. TheN
cocco/ithomorpha coccoliths are still tightly bound in analmost complete coccosphere, and so the likelihood of it
representing agglutination is negligible. There are also
other specimens in possible transitional states showing
Neosphaera coccoliths on a Cerato/ithus coccosphere or
hoop-like coccoliths on a Neosphaera coccosphere,
however, these are less convincing. If in the future thisrelationship is confirmed, N coccolithomorpha has priority
over C. cristatus, and so Ceratolithus would become ajunior synonym of Neosphaera.

NANNOFOSSll.,S OF THE MAASTRICHTIAN-PALEOCENEGERMAV FORMATION, SOUTHEAST ANATOLIA, TURKEY
Seving Ozkan and D. A/tiner
Topics: Maastrichtian-Paleocene, SE Turkey, Biostratigraphy

A great number of samples from the Germav Formation in
the SE Anatolia, Turkey, were examined for biostratigraphic purpose. The Germav Formation, spanning Early
Maastrichtian-Paleocene interval, mainly consists ofgreenish to yellowish grey shales, marls with intercalations of argillaceous limestones, siltstones and sandstones.
'This investigation is based on an analysis of samples
collected from 4 stratigraphic sections: GER-A and GER-C
sections from the GercOs area, SW Siirt; GA and GB sections
from the Kahta area, NE Adiyaman. Nannofossils are rare
to abundant, generally well-diversified and moderately
preservt:d. The recorded nannofossil events are calibrated
with equivalent planktonic forarniniferal zones alreadyrecognized in the same samples (Ozkan and Altiner, 1987;
Ozkan and Ozcan, in preparation) and high resolution
biostratigraphic zonation will be presented and discussed.
Preliminary data on the calcareous nannofossil
assemblages in the Germav Formation indicate a "transitionzone" at the Kif boundary interval.
REFERENCES
Ozkan S. and Altiner, D., 1987. Maastrichtian planktonic
Foraminifera from the Germav Formation in Gerciis area
(SE Anatolia, Turkey), with notes on the
suprageneric classification of globotruncanids. Revue dePaleobiologie, 6, 262-277.

CALCAREOUS NANNOFOSSll.,S FROM CALVELLO BASIN(SOUTHERN APENNINES, ITALY)
Filomena Orne//a Amore
Poster session
The Plio-Pleistocene sediments of the Calvello basin(Lucania, South Italy) have been investigated. They
represent part of wider basins whose remnants

discontinuously outcrop within Campano-lucano segment==========================46of the Apennines chain. A biostratigraphic analysis for these
terrigenous sediments, by means of calcareous nannofossils,
planktonic foraminifera and ostracods has been performed(Amore et al.,1994). The zonal schemes proposed forJournal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Mediterranean Sea by Rio et al.,('90) and Rio et al.,('94)
modified have been adopted in this study. The integrate
biostratigraphic and field study of the basin fill allowed torecognize for the first time three cycles: I) Lower Pliocene
in age (MNN 16a; MPl 4a Zones): G/oborota/iapuncticu/ata and Sphaeroidine//opsis sp. occur; IT) Middle-Late Pliocene in age (MNN 16b, MNN 17; MNN 18; MPl
Sa, b Zones p.p.): Discoaster pentaradiatus, D. surcu/us
among calcareous nannofossils and G/oborota/ia
bononiensis, G. crassafonnis among planktonic foraminifera
occur; Ill) The occurrence of G/oborota/ia injlata and G.
oscitans among foraminifera in the basal part of thesequence allowed to refer it to Late Pliocene (MNN 18,
MNN19a p.p. ; MP16 Zones). The P-P boundary has beenrecognized at about 75m from the bottom of the lastsequence by the FO of Gephyrocapsa caribbeanica s.I.
and an increase of Neogloboquadrina pachyderma left
coiled; in the topmost samples G. oceanica s.I. (MNN 19bp.p) occurs. Nannoflora assemblages are generally
abundant and well preserved. Quantitative analysis carriedout on nannoflora assemblages allowed to recognize,
according to the Mediterranean biozonal schemes, someevents also in the near-shore sediments of the Calvellobasin. In particular: LO ofDiscoaster pentaradiatus, shortly
before the LO of Globorota/ia bononiensis; FO of medium

sized (4,0-5,5 J.Lm) Gephyrocapsa, FO of G. caribbeanica
s.l. and FO of G. oceanica s./. (sensu Raffi et al. ,1993) wererecognized. Changes in surface water temperature havealso been recorded by means of the variation in theabundance of the cool-water Coccolithus pelagicus(Mclntyre and Be, 1967).
REFERENCES
Amore 0 ., Ciampo G., Di Donato V., Eposito P. and Staiti D.,
1994: Biostratigraphy and evolution of the Plio-Pleistocenic
Calvello basin (Potenza, Italy). Atti 77 - Congr. Soc. Geol. It.
-Riassunti, pp. 195-199.
Maclntyre A., and Be A.W.H ., 1967 : Modern
coccolithophoridae of the Atlantic Ocean. Deep Sea
Res., 14, 561-597.
Raffi 1., Backman J ., Rio D. and Shackleton N.J., 1993 :Plio-pleistocene nannofossil biostratigraphy and calibration
to oxygen isotope stratigraphies from deep sea drilling projectsite 607 and ocean drilling program site 677.
Paleoceanography, 8, 3, 387-408.
Rio D ., Raffi 1., and Villa G ., 1990: PliocenePleistocene calcareous nannofossils distribution
patterns in the western Mediterranean. Proc. ODP,
Sci Res., 107,513-533.
Rio D., Sprovieri R. and Di Stefano E. , 1994: The GelasianoStage: a proposal of a new Chronostratigraphic Unit of the
Pliocene Series. Riv. It. Strat., 100, 1, 103-124

PRODUCTION, SEDIMENTATION AND PRESERVATION OF
COCCOLITHOPHORES IN THE NORTHERN NORTH ATLANTIC
Hara/d Andru/eit
Monday, 10.45
Coccolithophores form a main part of the modern
phytoplankton in the northern North Atlantic. Theirremains in the sediments are frequently used for
paleoceanographic reconstructions. In this study theoccurrence of coccolithophores in the photic zone, in thewatercolumn, and in the surface sediments were
investigated to evaluate alteration processes.
About 200 watersamples from 80 stations were collected
since 1988 in the entire area. Additionally, two annual
sediment trap moorings from the Greenland Sea (1990-1992)
and one mooring from the Norwegian Sea ( 1991-1992) withtraps at 500 m, 1000 m, and 3000 m water depth were
investigated. Samples of the surface sediments, underlying
the sediment traps, were also examined.
The sites of the sediment traps are located in the distinct
oceanographic regimes of the Arctic domain (GreenlandSea, to the west) and the Atlantic domain (Norwegian Sea,
to the east) and are separated by oceanographic frontal.
systems.
Regional species groups can be defined according to
species temperature-tolerances (Sarntleben et al. 1995). The
distribution of these groups coincide with the main surface
water masses. However, the coccolithophore communities
exhibit a high variability linked to seasonality. The variationin species composition and cell densities is most impressively========================~47

illustrated by the enormous blooms of Emiliania huxleyi.
The examination of sinking assemblages from thesediment traps reveals that inspite of alteration by
sedimentation processes, a distinct seasonal pattern canstill be seen. The coccolithophore flux in the Norwegian
Sea is about 10 to 20 times higher than in the Greenland
Sea. From east to west the diversity diminishes and a changeof the dominant species from E. huxleyi to Coccolithus
pelagicus occurs.
To compare the living communities and sinking
assemblages on a joint basis, the coccolithophore countsof the watersamples were grouped according to the regional
distribution. This resulted in an averaged community for a
specific area which can be compared with the annual
averaged assemblages of the sediment traps and with thelong term record of the fossil assemblages in the surface
sediments.
REFERENCES
Samtleben, C., Schafer, P.,Andruleit, H., Baumann,A,Baumann,
K.-H., Kohly, A, Matthiessen, J., SchrOder-Ritzrau, A,'Synpal' Working Group (1995): Plankton in the NorwegianGreenland Sea: from living communities to sedimentassemblages- an actualistic approach.- Geol. Rundsch., 84:
108-136.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

SEDIMENT TRAP STUDIES OF COCCOLITH AND PLANKTONICFORAMINIFERAL FLUXES IN THE BENGUELA UPWELLING SYSTEM
Jacques Giraudeau and Geoffrey W. Bailey

Monday, 16.50
Coccoliths and planktonic foraminifera collected by asediment trap deployed on the upper slope offWalvis Bay,
Namibia, were investigated in order (1) to assess theircontribution to the total particulate flux, (2) to evaluate
their response to seasonal changes in the dynamics of the
Benguela upwelling process, and (3) to use them as tracersof particle transfer process on the slope. The trap, locatedat 545 m depth, 50 m above the sea floor, provided highresolution (8 days) times series samples from late winter toearly summer. This 4-month period is marked by a drasticchange in hydrological processes, from active to quiescent
upwelling conditions. The total mass flux ranged from 3 to
1, lg/m 2 /day. The litho genic fraction was the main
contributor to the total mass flux (64% of averagecontribution), followed by carbonate (22%), organic matter(8%), and biogenic opal (5%). The relative contributionsof the four components to the total mass flux were relatively
stable throughout the period of the experiment, thereby
suggesting that seasonal changes in hydrologicallupwelling
process, from late winter to early summer, did not induce
sharp modifications in the composition of the particles
sedimenting on the slope. The bulk oflithogenic particles
sedimenting on the continental margin originates fromaerosol sand plumes due to katabatic wind events.
Considering the low frequency and short duration of such
events, we suggest that resuspension of shelf material andcontinuous horizontal advection to the slope werenecessary to account for the high contribution oflithogenic
particles recovered by our trap throughout its 4-monthdeployement.
The free-coccolith mass flux closely followed total massflux variations, and ranged from 90 to 10 mg/m2 /day, thereby
accounting for less than 10% (on an average) of the total
biogenic carbonate mass flux. Coccolith number fluxes
varied from 4200 106/rn2/day to 400 106/m2 /day, Emi/iania
huxleyi being the dominant form (relative abundance: 60
to 75%). On the contrary to coccolith fluxes, thecoccosphere fluxes did not show any significant
covariations with total mass fluxes. This, coupled, with
dissimilarities in species assemblages, suggest that the bulk
coccolith fraction and the coccospheres were affected by
distinct transfer process: lateral transport of coccoliths
resuspended from the shelf, vertical advection of
coccospheres from the overlying surface waters.
Planktonic foraminiferal number fluxes, dominated byjuvenile specimens, ranged from 600 to 50 103/m2/day, androughly followed the total mass flux variations. The threesize classes Uuvenile, neanic, adult) presented distinct
patterns in flux variations, which can be related to distinct
transfer process, as well as mass mortality events in thecase of the adult populations.

OCEANIC FRONTS IN THE MESOZOIC
Wil/iam W. Hay

Poster session
The modem ocean is characterized by four regions, threeof which are mirrored in each hemisphere: an equatorial
belt (28% of the ocean surface area) characterized bydivergence and shared by the two hemispheres, stratified
tropical-subtropical anticyclonic gyres (46%), temperate
mid-latitude belts of water characterized by convergenceand steep meridional temperature gradients (11%), anddeeply convecting polar oceans characterized by cyclonic
gyres (13%). Convergence and divergence of the ocean
waters are forced beneath zonal winds. Convergences orfronts form sharp boundaries between water masses andintroduce surface water into the ocean interior. The fronts
can be recognized by abrupt changes in nannoplankton
assemblages. The sites of divergence are more diffuse; they
separate water masses and return water from the oceaninterior to the surface. Surface waters of the equatorial belt
flow westward, driven by the easterly trade winds. Eastward
subsurface flow returns some of the water, but much of the
westward flow becomes incorporated into the westernboundary currents of the tropical subtropical gyres.

Increasing zonal velocities of the trade winds away fromthe atmospheric Intertropical Convergence Zone (ITCZ)========================~61

induce divergence and upwelling in the waters of theequatorial belt. The most stable features of the modem
ocean are the stratified tropical-subtropical gyres between
15° and 45° Nand S. Low-latitude easterly trade winds andmid-latitude westerly winds drive the gyres. They also force
convergence in the gyre centres. The sinking waters spreadbeneath the gyre as central waters. The maximum of thezonal component of the westerly winds occurs at about 45°
N and S. The zonal winds induce meridional flow of thesurface waters toward the equator, forcing sinking along
the subtropical and polar fronts and forming barriers topoleward heat transport. The subtropical front is the source
ofthermocline water. Intermediate water forms by sinking
along the polar front. The alternate, competing, source forintermediate water is outflow from saline marginal seas.
Decreasing zonal wind velocities poleward of the polar
fronts induce divergence, cause cyclonic circulation, andpromote deep convection and deep water formation.
The Jurassic and Early Cretaceous ocean may havebeen similar to that of the present, but the late Cretaceous
ocean was significantly different, with polar temperatures
well above 5° C. The tropical-subtropical gyres in theJournal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

THE TURNOVER OF CALCAREOUS PHYTOPLANKTON FROM mE
BARREMIAN- APTIAN BOUNDARY INTERVAL IN NW EUROPE
Gregor Bischoff and J6rg Mutterlose
Poster session

In NW Europe and elsewhere the Barremian-Aptian
boundary interval is marked by a major change of thepaleoceanographic setting. Due to a widespreadtransgression in the earliest Aptian paleoceanographic andsedimentary patterns changed both in NW Germany andin S England. A major floral and faunal turnover occurs at
the Barremian-Aptian boundary interval. Restrictedconditions prevailing in the latest Barremian and earliest
Aptian, which are expressed by anoxic sediments, changed
to a pelagic setting in the late early Aptian. The compositionof calcareous nannofossil assemblages, however, does notchange abruptly. The main results of an integrated
multidisciplinary study may be summarised as follows:
1. Nineteen nannofossil events (first occurrences, last
occurrences, acmes) characterize the late Barremian to early
Aptian sediments of NW Europe. Most of these events
can be recognized throughout NW Europe (NW Germany,
North Sea) and allow a correlation throughout the NorthSea.

2. There is a general shift from endemic assemblages
dominating in the Barremian towards cosmopolitan onesin the Aptian.
3. The extinction and the onset of new floras is spreadthroughout the earliest Aptian. The biological turnover isgradually.
4. The first new cosmopolitan species (C. litterarius, R.
irregularis, E. flora/is, F. oblongata, R. angustus) occur
well below the significant sedimentological change(Fischschiefer).
5. The calcareous phytoplankton of the early Aptian
Fischschiefer suggests deposition under warm waterconditions during a regressive phase.
6. The Fischschiefer, an organic-rich sediment depositedunder anoxic conditions, is considered to be a regional
phenomenon. Data from organic geochemistry suggest
rather preservation than productivity as the cause for theblack shale sedimentation.
It has been suggested, that increased spreading rates
and abnormal intraplate volcanism in the Aptian may havecaused the onset of the mid-Cretaceous greenhouse. This
would have caused global warming, high humidity andsluggish oceanic circulation, resulting in an accelerated
carbon cycling and increased availability of nutrients. Ourdata, however, do not support the idea of higher
productivity. Thus it seems more likely to explain the floral
and faunal turnover by changes of the sea level and changes
in the circulation pattern of the epeiric NW-European sea.

JURASSIC- EARLY CRETACEOUS CALCAREOUS NANNOFOSSILS FROM THE
NEUQUEN BASIN, ARGENTINA
P.R. Bown and C. Ellison

Wednesday, 12.25
A preliminary summary of calcareous nannofossil resultsfrom Jurassic and Cretaceous sediments of the Neuquen
Basin (Neuquen and Mendoza Provinces), Argentina, ispresented. Ninety five samples were collected fromformations ranging in age from Pliensbachian to Hauterivian.
Seventy samples yielded calcareous nannofossils. The
assemblages are generally of low abundance andmoderately-well to poorly preserved. All assemblages are
dominated by Watznaueria, althoughMicrantholithus iscommon in Lower Cretaceous sediments. Biostratigraphic
dating of the assemblages is problematical due to theabsence of most marker species although higher diversity
in the Toarcian-Bajocian and Tithonian-Hauterivian haveprovided broad dates. Biogeographical observations arealso limited due to the low diversity, however, a significant
result is the absence of Nannoconus in Tithonian to Lower
Hauterivian sediments and only rare nannoconids in theUpper Hauterivian. This contrasts with high nannoconid
abundances in the western Tethys-Caribbean region at thistime and provides tenuous support for the existence of anAustral nannofloral realm through the late Jurassic-early
Cretaceous interval.

COCCOLITH BUILDING BLOCKS: IDGH RESOLUTION ANALYSES OFIIETEROCOCCOLim MORPHOLOGY AND CRYSTALLOGRAPHY
P.R. Bown, J .R. Young, T.E. Ehrendorfer, S.A . Davies, JM Didymus and S. Mann
Poster session

High resolution analysis of coccolith structure has beenachieved using a number of different but complimentary
analytical techniques, namely, light microscopy (LM),scanning electron microscopy (SEM), high-resolution
transmission electron microscopy (HRTEM), and selectedarea electron diffraction (SAED). This study is the firstwhere single coccoliths (and single crystals within===========================48

coccolith structures) have been examined using each of
the techniques in turn. Since each method contributes
information ofa different nature and accuracy, and is limited
by different factors, their combined use allows a high degreeof confidence where the same results were achieved.
Furthermore, additional data beyond the limitations ofindividual methods were obtained.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

We present detailed results from the analysis of
Emiliania huxleyi and Biscutum magnum and moregeneral results from a range of heterococcolith families.
We conclude that: (i) The marginal area (rim) of
heterococcoliths consist of only two discrete
crystallographic units, despite the gross morphologicalappearance of a complicated multi-cyclic architecture.
These findings support the V /R hypothesis of Young et al.
( 1992) which predicts that only two crystallographic units
constitute the entire coccolith- these units originating froma common nucleation site in the proto-coccolith ring. (ii)
The two crystallographic units have considerably different
c-axis orientations but the c-axes in neither unit are truly
vertical or radial. In Biscutum magnum, for example, one of
the units has a c-axis inclination of about 60°-70° and an
azimuth -45° anticlockwise. In the second unit the c-axis
has an inclination of0°-l0° and deviates from the radial

Journal of Nannoplankton Research, I 7, 2, 1995.

direction by -20° clockwise. These orientations are very
approximately vertical and radial but are still significantly
different from the orientations predicted in the originalmodel. One interesting result of this is that the chirality ofcomplete coccoliths can now be seen to be determined by
nucleation processes. (iii) The analysis of other coccolith
species in different phylogenetic groups reinforces these
conclusions; two crystallographic units are consistently
present but that the values of the c-axis inclination andazimuth are more variable than initially predicted. The
consistency of the basic pattern provides strong support
for the interpretation of heterococcolithophorids as amonophyletic group. The variability of orientations makes
identification of homologous units less straightforward but
ip.creases the significant phylogenetic characters that canbe determined.

ALBIAN/CENOMANIAN TO KIT STAGE BOUNDARIES AND NANNOFOSSIL
EVENTS: INCREASED PRECISION IN UPPER CRETACEOUS NANNOFOSSIL
BIOSTRA TIGRAPHY AND CORRELATION
Jackie Burnett
Poster session
In Brussels this September, Cretaceous stage boundary
stratotypes will be designated for the Cretaceous. The
boundaries themselves will be defined by an event, probably
biostratigraphical but probably not based on nannofossils(since nannofossils cannot be seen in the field).
Nevertheless, these decisions will provide a more precise
framework within which correlation between nannofossil(sub-) zones and (sub-)stages can be improved.
At present, the assignment of stage names tonannofossil zones is imprecise, particularly at/around stage
boundaries, because stage boundaries have not previously
been strictly defined. Confusion abounds in the literature:investigators of onshore sections tend to use macrofossil
biostratigraphy, which has been correlated to stages at least
on a regional level, to provide a time-frame for theirnannofossil zones, whilst investigators of oceanic cores, inthe absence of macrofossil biostratigraphy, use nannofossil
events to define, rather than approximate, the stage
boundaries.

Study of numerous sequences, both onshore andoceanic, and including a number of proposed stage
boundary stratotypes, has provided integrated sequencesof fossil (macrofossil, microfossil and nannofossil) andgeochemical events across the Albian/Cenomanian to KIT
boundary intervals. Primarily, the study set out to more
rigorously define the stage boundaries and the ages ofSissingh 's/Perch-Nielsen's nannofossil (sub-)zones,
following the original stage boundary conference(Copenhagen, 1983 ). The geographical andbiostratigraphical extent of the study, however, also
indicated previously unused nannofossil events, andprovided an increased resolution between events
previously believed to have been contemporaneous. Thus,
the CC zones have been refined and revised.
These results will enhance precision in correlation
between nannofossil zones and other stratigraphies, andprovide a higher resolution in nannofossil biostratigraphy
for the Upper Cretaceous.

SOME CALCAREOUS NANNOFOSSILS MISINTERPRETED IN LITERATURE ASTETRALITHUS, TRIQUETRORHABDULUS, FUSELLINUS SP. ARE ACTUALLYSPICULES OF DIDEMNUM SSP. (TUNICATA, ASCIDIAN). EVIDENCE FROMUPPER JURASSIC SEDIMENTS OF CHARENTES (W. FRANCE)
Georges Busson, Denise Noel, Fram;oise Monniot and Annie Cornee
Poster session
In the Upper Jurassic ofCharentes (S. W. ofFrance), in alimestone-mart rhythmic sedimentation system, the finecarbonate fraction of the marly interbeds is largely
constituted of some micron-sized nannoliths either fusiform
or composed of several conical points. We regard them as

spicules of Didemnum ssp. for the following reasons.

========================49

1- By their wide morphological variety, the spicules arequite similar to the tunic spicules extracted from the type ofthe living species Didemnumfusiferum VAN NAME 1921
that we have studied in SEM. They also look like thespicules of D. minutum BONET et BENVENISTEVELASQUEZ.1971, described from Callovian sediments inJournal of Nannoplanlcton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Mexico. The nomenclatural problem of the spicules isdiscussed.
2- Indeed, aragonitic crystallisations resembling
Didemnidae spicules can be obtained in vitro but, inexperimental conditions, which try to duplicate the physicochemical conditions prevailing in the tunic of the living
animal. In the contrary, by some examples, we show that inrecent and ancient sediments from various aquatic
environments, the observed aragonitic - and sometimes
calcitic- chemical or biochemical precipitations are different
from Didemnidae spicules.
3- We emphasize the necessity to take into accountthe whole association of spicules present in a given
sediment to state their Didemnidae origin. Only someisolated spicules are not enough to state such origin.
Didemnidaespicules are rarely recorded in sediments.
We show that some of them could have been misinterpreted
as calcareous nannofossils attributed to the following genera: Tetralithus (Gardet, 1955), Triquetrorhabdulus (Martini,1965), Fusel/inus(Noel1956).
REFERENCES
Bonet F., Benveniste- Velasquez N. (1971 ). -Espiculas deAscidias fosiles y actuales. -Rev. Inst. F Mexicano Petrol. ,3 (4), 8- 35.
Van Name W. G. (1921).- Ascidians of the West Indian Region
and Southeastern United States. Bull. Amer. Mus. of Nat.
Hist., 44, 16,283-494.

COCCOLITHUS PELAGICUS, A SORT OF PRODUCTIVITY PROXY?
Mario Cachao and MT. Moita
Monday, 11.10
Data on the development dynamics and distribution
patterns of Cocco/ithus pelagicus the water column on
the Portuguese upwelling system and in sediments(coccolith present day and Quaternary taphocoenosis) fromthe Portuguese continental margin and Western
Mediterranean (ODP 653 Pliocene section) may bequestioning the traditional interpretation of C. pelagicus
as a cold water proxy. Our results suggest instead an
opportunistic behaviour of Cocco/ithus pelagicus to
newly nutrient enriched waters (by upwelling or otherprocesses), but outside areas of strong turbulence.
Cocco/ithus pelagicus is one of the few extant
Nannoplankton species which are easy to identify fromboth a biological (coccospheres from water column samples)and a paleontological (coccoliths from surface sediment
samples) point ofview. For this reason it should be possible
to understand the ecological behaviour of this species (orat least its heterococcolith-bearing phase) from available
laboratory and biogeographic data together with its
sedimentary record on continental shelf and abyssal planes.
In addition its stratigraphic record covers practically all
the Cenozoic (-60 Ma), which means that, in theory, itspresent day ecological/oceanographic meaning could betraced back till the Paleocene.
Based upon its present day biogeography, mainly
restricted to North Atlantic subpolar water masses (inoceanic domain, MCINTYRE and BE 1%7), there seems to
be a general agreement that C. pelagicus, characterises
cold water masses (living interval-1, 7° to 15°C, OKADA
and MCINTYRE 1979, WINTER et al. 1994; optimum
interval2° to l2°C, OKADAand MCINTYRE 1979). Since
then it has been used as a qualitati\le/semiquantitative
parameter (RAFFI and RIO 1981), in transfer functions(GIRAUDEAU and PUJOS 1990) and/or in Factorial
Analysis (HAQ 1980) interpretations as a paleotemperature
proxy. Nevertheless some authors have also recognised on
it a signal of nutrient rich surface oceanic waters(MCINTYREandBE 1%7, RAHMAN andR01H 1990). In
surface waters temperature and nutrient concentrations arestrongly covariant and it is not clear which of the two
properties may influence the most the development C.
pelagicus.

Along the Portuguese continental margin, from 42°N
(Caminha) to 37°N (Algarve), C. pelagicus is almost always
present in water column samples, although in low
concentrations (normally below 1000 cell /I). Its distribution
can be better described as being related to the area
influenced by a water body of subtropical characteristics(ENAWT inRlOS et al. 1992) which is modified in upper
layers. The abundance of C. pelagicus decreases
northward, along the western coast, apparently inaccordance with a progressive change of ENAWT
characteristics. In fact its minimum values were observed incoastal waters to the north ofNazar canyon (39,5°N}, anarea which during Spring and Summer tends to be occupied
by a shallow lens of reduced salinity, resulting from NE
Atlantic and Bay of Biscay waters combined with local
riverrunoff(JORGE DA SILV A and MOITA 1993).
On an upwelling coastal region such as the Portuguese
margin, phytoplankton assemblages can be positioned along
an axis relating its different groups and species to decaying
turbulence and nutrient availability (MARGALEF 1978).
On the core of upwelling, species with maximum growth
rates, such as Diatoms, take advantage, contrasting withassemblages from offshore nutrient-poor and stratified
waters, such as Dinoflagelates with lower growth rates. In
these regions Coccolithophores appear to occupy anintermediate ecological position between those two groups(ESTRADA and BLASCO 1985). In this context our data(from two areas of distinct upwelling patterns: August 1985
at the S. Vicent Cape- 37°N- ; August 1987 at Northwestern coast - 41 o 05 'N) show that in both cases C.
pelagicus occupies a confined band, at the immediate
border (upwelling thermal front) of the turbulent fertile core,
between Diatoms which clearly dominate the upwelling
center, and an outer area occupied by other .
Coccolithophore species (e.g. Calcidiscus leptoporus,
Helicosphaera carteri). The development dynamics of C.
pelagicus during an upwelling event at North-western
coast (41°05 'N), revealed an increase of cells in response tonutrient enrichment, with maximum values being observedin the picnocline- nutricline, below the wind-driven layer.
When present in waters with subtropical characteristics
50========================~

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

C. pelagicus reveals some affinity for relatively low
temperature conditions, the maximum numbers being
obtained for the interval 13 ° to 15°C, during the upwellingseason. Our results also show that this species occupies an
ecological niche between diatoms and other
Coccolithophores. It reveals an opportunistic behaviour
for nutrients and moderate turbulence (and not simply"coldwater") which also may explain its present day North
Atlantic biogeography, between K-assemblages on
stratified water masses brought northwards by Golf Stream,
and turbulent polar waters characterised by E. huxleyi anddiatoms (BRAND 1994, OKADA and MCINrYRE 1979).
Another interesting pattern could be disclosed after
the analyses of 70 surface samples collected from Northwestern section of Portuguese occidental continental
margin. These results showed that significant increases in
the percentage of C. pelagicus on the total nannolithpresent day taphocoenosis were directly related to thepresence of three river mouths. We interpreted this as aconsequence of"fresh" input of nutrients from river runoff
which seems to favour ("opportunistically") this species.
The results from the Atlantic coast of Iberian Peninsula
allow us to conclude that C. pelagicus is somehow related
to nutrient availability and productivity. Consequently it
is useful to test this conclusion with other productivity
proxies, in other regional context. When we compared C.
pelagicuswith8 13 CG.e1ongatus +G.ob"uquur WesternMediterranean
Pliocene (4.85 to 1.95 Ma) time series several match (sametrend) and unmatch (opposite trend) intervals wererecognised. Unmatch intervals (with 600 to 200 Ky) occur
just before particular moments (when significative changes
in planktonic Forarninifera assemblages take place) after
which a predominantly match interval is registered. It seems
that when long-standing ("mature and stratified ?") pelagic
Mediterranean paleocommunities persisted, preferential
development of C. pelagicus was related with episodes oflow general productivity. After particular moments, when
renewing of the pelagic paleocommunities occurred in the
Tyrrhenean Sea, C. pelagicus started to contribute

Journal of Nannoplankton Research, 17, 2, 1995.

(preferentially, as an opportunistic species) directly to thegeneral productivity, for a certain period of time, before
returning to the earlier pattern of development.
REFERENCES
Brand, L., 1994: Physiological ecology of marine coccolithophores,
in Winter, A. and Siesser, W. (Eds), Coccolithophores,
Cambridge Univ. Press: 39-49.
Estrada, M. and Blasco, D., 1985: Phytoplankton assemblages incoastal upwelling areas, in International Symp. Upwelling of
W. Africa, C. Bas, R. Margalef and P. Rubias (eds), Inst.
Invest.Pesqueras, Barcelona: 379 - 402.
Giraudeau, J. and Pujos,A, 1990: Fonction de transfert basee surles nannofossiles calcaires du Pleistocene des Carabes,
OceanologicaActa 13 (4): 453-469.
Haq, B.U., 1980: Biogeographic history of Miocene
calcareous nannoplankton and paleoceanography of, the Atlantic Ocean, Micropaleontology 26: 414-443.
Jorge Da Silva, A and Moita, M.T., 1993: Dynamic of Toxic
Dinoflagellates during an upwelling event at the northwest
coast off Portugal, Int. Counc. Explor. of the Sea (ICES),
paper L:66: 11 pp.
Margalef, R., 1978: Life-Forms of Phytoplankton as survival
alternatives in an unstable environment, Oceanolog. Acta 1(4): 493- 509.
Mclntyre, A. and Be, A., 1967: Modern Coccolithophoresof the Atlantic Ocean - I. Placolith and Cyrtholiths,
Deep-Sea Res., 14: 561 - 597.
Okada, H. and Mclntyre, A, 1979: Seasonal Distributionof Modem Coccolithophores in the Western North Atlantic
Ocean, Marine Biology, 54: 319-328.
Rahman, A. and Roth, P.H., 1990: Late Neogene
Paleoceanography and Paleoclimatology of the Gulfof Aden region based on Calcareous nannofossils,
Paleoceanography, 5 (1): 97 - 107.
Rios, A., Perez, F. and Fraga, F., 1992: Water masses in
the upper and middle North Atlantic Ocean east of the
Azores, Deep-Sea Res. 39, 3/4): 645 - 658.
Winter, A.; Jordan, R. and Roth, P ., 1994: Biogeography ofliving Coccolithophores in ocean waters, in Winter, A.
and Siesser, W. (Eds), Coccolithophores, Cambridge Univ.
Press: 13- 37.

AN EXAMINATION OF THE GLOBAL RELATIONSHIP BETWEEN THE LAST
TWO "SPECIES" OF DISCOASTERS AT THE END OF THE PLIOCENE
A/ex Chepstow-Lusty and Mark Chapman
Monday, 12.00
high resolution records of Discoaster abundances using 8
sites (Fig. 1) from the Atlantic (DSDP 552, DSDP 607, ODP
658, ODP 659 and ODP 662), the Pacific (0DP677 and ODP
806), and the Indian Oceans (ODP 709).
A uniform chronology, based on the orbitally-tuned
oxygen isotope stratigraphy from ODP Site 677, is employed
for each site. High resolution records of Cocco/ithus
pelagicus are also examined at ODP sites 677, 709 and 806
to provide an independent assessment of the effects ofvariable dissolution on Discoaster abundances. In spite of
the observed marked temporal and spatial fluctuations inabundance, it appears that there is generally a consistent
relationship between these two "species" which cannot be

Discoasters are the enigmatic calcareous remains of a groupofphytoplankton spanning 55 Myr of the oceanic record
from the Upper Paleocene to the Upper Pliocene,
disappearing at approximately the base of the Olduvai
subchron, 1. 95 Ma. In the 200 kyrs prior to extinction, athree-armed form called Discoaster triradiatus is produced.
This taxon occurs globally and in significant abundances
relative to the dominant surviving species Discoasterbrouweri. Here, we examine the extent of the eo-variation
between these two morpho-species, and assess if thisrelationship is merely the response of a single biological
species to the accentuation of glacial-interglacial climatic
variability during the late Pliocene. We have produced51

Journal of Nannoplankton Research, 17, 2, 1995.

J

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

PACIFICINDIANATLANTIC

Figure 1: Location of sites investigated in this work.

attributable to differential preservation. This suggests thatthe ecological preference of discoasters for warm, lownutrient waters is the major factor controlling theirdistribution. The detailed analysis of D. brouweri andD. triradiatus records in this study, as shown for ODP Site
709 (Fig. 2), clearly demonstrates that the D. triradiatus
acme is a useful biostratigraphic datum which can beapplied globally.

1.5

SITE 709

D. brouwerl/mm2

J1.95-2.16 Ma •

Q5

N

Q

u

t.l

90

~.

t

ci
0

... ..

~

so.: .. .

.• ..

rvvc:~·%
12

2

1.1

Coccolithu~

2IXI

I 1-

r = -0.45

1.95-2.16 Ma

u

:l
0

:

as~ ..
0.

(jpelagicus

'

/mm2

100

- - ..

D. brouwerVmm2

1.1

~j

r = 0.69

J- - ..

I • •I.

D. brouwerVmm2
c

...

12

Age (Ma)
Figure 2: Abundance variations and correlation of Discoaster brouweri, Discoaster triradiatus and Coccolithus pelagicus at ODP Site 709.

==========================52

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995.

COCCOLITHOPHORID DISTRIBUTION ACROSS A TRANSECT BETWEEN THE
ffiERIAN PENINSULA AND THE BALEARIC ISLANDS(NORTHWESTERN MEDITERRANEAN SEA)
Lluisa Cros
Monday, 11.35
To study the coccolithophorid distribution in the CatalanoBalearic Sea and its relationship with the different water
masses and hydrographic structures, samples at surface andat 40 m. depth have been taken along a transect between
Barcelona and the threshold between Mallorca andMenorca. The water samples were collected aboard the
Oceanographic Ship Garciadel Cid (May 31th- June 16th)and hydrographic parameters were measured in the same
stations. This report presents a preliminary study of thecoccolithophorid assemblages found as well as thecomparison of some results between different sample
preparation methodologies.
The samples were fixed aboard the ship withformaldehyde neutralized with hexamethyl-enetetramine
and then filtered at the laboratory. In three stations of thetransect, parallel samples were filtered on board. The
samples treated with this last method showed the best
preservation of coccolithophorid specimens.
Three different surface water masses separated by two
fronts, can be recognised between the Iberian Peninsula
and the Balearic Islands. Near the Iberian Peninsula there
are a low salinity coastal water influenced by continental

discharges. At the Balearic Islands side there are a warmer
and well-stratified water mass of Atlantic influence. In the
middle, a high salinity Mediterranean Sea water is present.
Emiliania huxleyi was the most abundant andubiquitous species found. Syracosphaera pulchra as wellas the majority of Syracosphaera species were moreabundant in the continentally influenced coastal water
masses, near the Iberian Peninsula. Gephyrocapsa ericsonii
increased towards the Balearic Islands. Gephyrocapsa
mullerae, the other species of Gephyrocapsa found,appeared in the water mass of Atlantic influence where G.
ericsonii had the maximum. Rhabdosphaera c/avigera,
Rhabdosphaera xifos, Polycrater ga/apagensis andUmbellosphaera tenuis increased towards the Balearic
Islands too. All the specimens ofRhabdosphaera clavigera
belonged to the form R. clavigera var. stylifera. It isinteresting to point out that the only form of Calcidiscus
leptoporus found was C. /eptoporus f. rigidus, which
occurred in the vicinity of the Balearic Islands. The greatest
number of holococcolithophorid species as well as the
maximum coccolithophorid species diversity were found in
the station nearest to the Balearic Islands.

CALCAREOUS PLANKTON BIOSTRA TIGRAPHY AND 40 ARf9 AR DATING OF
VOLCANIC ASH LAYERS FROM MONFERRATO (NW ITALY)
A. d 'Atri, A. Novaretti, R. Ruj]ini, MA. Cosca and J. C. Hunziker
Poster session
In the last years many volcano-sedimentary beds have been
discovered in the Oligo-Miocene succession of the
Monferrato (NW Italy). They are made up ofvitric tuffs
and contain minerals suitable of radiometric age
determination.
Petrographically, they show vitroclastic texture withwell preserved glass shards and phenocrystic assemblage
including plagioclase, quartz, sanidine, biotite, minor
amphiboles and pyroxenes.
Two volcaniclastic layers (Villadeati and Varengo),
bearing well preserved biotite and amphibole, have beenchosen for biostratigraphic studies and 40Ar /3 9Ar dating.
A quantitative analysis of calcareous nannofossil
associations present in the volcaniclastic layers and in theunder- and overlying sediments has been carried out. The
Villadeati layer can be attributed to the lower part of Zone
CN2 (Okada and Bukry, 1980) and/or to Zone MNN3a (S.
belemnos) ofFornaciari and Rio ( 1995), Late Burdigalian in============================53

age. The Varengo layer falls within the upper part of Zone
CN3 (Okada and Bukry, 1980) and/or the upper part ofZone MNN4a (H. ampliaperta - S. heteromorphus) of
Fornaciari and Rio (1995), correspondent to Early Langhian.
The forarniniferal data confirm this attribution; in fact theVilladeati and Varengo layers are respectively referable tothe lower part of Zone N7 (Late Burdigalian) and to thelower part of Zone N8 (Early Langhian) of Blow (1 %9).
40Ar/39Ar analyses performed with the step heating
technique at the University ofLausanne have been carriedout on amphibole and biotite from the two ash layers.
Villadeati sample gives a plateau age of 18.7 ±0.1 Ma,
whereas Varengo sample gives a plateau age of 16.4 ±0 .2

Ma.
This radiometric data are in good agreement with thebiostratigraphic ones and will be very useful to calibratenannofossil- and foraminiferal bioevents in the
Mediterranean region.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Progranune and Abstracts.

PALEOCENE TO EARLY EOCENE CALCAREOUS NANNOFOSSIL
BIOSTRATIGRAPHY OF THE EL KEF SECTION (TUNISIA)
Eric de Kaenel
Tuesday, 11.10
A light microscopy study of 60 samples collected by Amoco
Paleontologists from a composite of two sections near El
Kef, Tunisia was completed in the summer of 1992. This
composite section of 430 meters spans the K!f boundary(in its type region) in shales of the El Haria Formation into
overlying lower Eocene limestones. The main objectives ofthis study were a revision of Paleocene to early Eocene
nannofossil taxonomy and an improved biostratigraphic
framem>rk. Perch- Nielsen ( 1981a) had demonstrated that a
relatively complete Paleocene section is present near El
Kef, recognizing Zones NP 1 through NP9 of Martini (1971 ).
Perch-Nielsen (1981 b) also subdivided Zone NP 1 into four
subzones based on the Tunisian material. The abundanceand diversity of nannofossil assemblages recovered bycentrifugation from the El Haria shales were high. The
excellent preservation and the continuity of section
provided further incentive to restudy sections from thisregion in reference to more recent advances within thepast one and one-half decade.
Martini (1971) published the first global nannofossil
biozonation of the Cenozoic (NP/NN Zones), whose
Paleocene to early Eocene zones were defined in various
outcrop sections in NW Europe and the circum-Caribbean,
as well as references to Tunisia and New Zealand. Romein(1979) studied individual lineages in coeval section (Spain,
Denmark, Sweden, Israel), reproducing the biostratigraphic
framework of Martini (1971) and enhancing resolution
within Zone NP 1. Okada and Bukry ( 1980) subsequently
published a Cenozoic nannofossil biozonation (CP/CN
Zones) based on deep-sea material. Interest in hydrocarbon
exploration in the North Sea resulted in enhanced
biostratigraphic resolution within the Paleocene (PerchNielsen, 1979; vanHeckandPrins, 1987; and Varol, 1989).
Varol (1989) extended this enhanced resolution into low to
mid latitude regions based largely on material from the
Kokaksu Section in Turkey, for which he defined 20
Paleocene nannofossil zones (NTpl-20). Bybell and SelfTrail ( 1995) improved understanding of the taxonomy andevolution of late Paleocene and early Eocene nannofossils
based on material from southern New Jersey (U.S.A. ).
Many of the nannofossil bioevents and lineages
recently described from the New Jersey sections (Self-Trailand Bybell, 1995) were independently observed in the El
Kef region and indicate the their potential utility in global
correlations. In addition, nearly all the calcareous
nannofossils bioevents described in the aforementioned

papers (including the North Sea) have been observed in
the composite El Kef section and integrated into a unified
biostratigraphic scheme. More than 290 nannofossil species
have been identified in the composite section, including
several new species recognized within evolutionary lineages.
A table summarizing the nannofossil biostratigraphic
framework is presented, as well as fifteen related tables
showing the distribution of species within individual 50
genera and their major morphologic characteristics. The
main lineages considered include: Bomolithus-Heliolithus,

Chiamolithus, Cruciplacolithus-Clausiccocus, Ellipsolithus, Neobiscutum-Futyania-Prinsius-Towieus,
Chiastozygus-Neochiastozygus,Fasciculithus,
Neocrepidolithus,Marka/ius-Discoaster, Palaeopontosphaera-Hornibrookina, and Sphenolithus.
REFERENCES
Bybell, L. M. and Self-Trail, J. M., I995: Evolutionary,
biostratigraphic, and taxonomic study of calcareous
nannofossils from a continuous Paleocene-Eocene
boundary section in New Jersey . U.S Geol. Survey
professional paper; 1954, 1-36.
Heck, S.E. van and Prins, B., 1987: A refinednannoplankton zonation for the Danian of the Central
North Sea. Abh. Geol. B.-A., 39, 285-303.
Martini, E., 1971: Standard Tertiairy and Quaternary
calcareous nannoplankton zonation. In A.Farinacci (Ed.),
Proc. ll Plankt. Conf., Roma, 1970, 2, Tecnoscienza,
Rome, 739-785.
Okada, H . and Bukry, D., 1980: Supplementarymodification and introduction of code numbers to the lowlatitude coccolith biostratigraphic zonation (Bukry
1973, 1975). Mar. Micropaleont., 5, 321-325.
Perch-Nielsen, K., 1981a: Les coccolithes du Paleocenepres de EL Kef, Tunisie et leurs ancetres . Cah.
Micropaleont., 3, 7-23.
Perch-Nielsen, K. , 1981 b: Nouvelles observations sur lesnannofossiles calcaires a la limite Cretace-Tertiairepres de El Kef (Tunisie). Cah. Micropaleont., 3, 25-37.
Romein, A. J. T ., I 979: Lineages in early Paeogene
calcareous nannoplankton. Utrecht Micropaleont.
Bull., 22, p. 1-231.
Varol, 0., I 989: Paleocene calcareous nannofossil
biostratigraphy. In S. van Heck and J. Crux (Eds.),
Nannofossils and their applications. London: EllisHorwood, 267-310.

CALCAREOUS NANNOFOSSILS BIOSTRA TGRAPHY OF THE PLIOPLEISTOCENE DEPOSISTS OF THE J»ELORITANI MOUNTAINS (NE SICILY)
Agata di Stefano
Poster session
Topics: Plio-Pleistocene, Southern Italy, Biostratigraphy

Plio-Pleistocene sediments crop out largely along the northeastern coast of Sicily, facing the Tyrrhenian Sea. A
quantitative analysis of calcareous nannofossils carried out
on 9 sections sampled in the easternmost sector of thePeloritani Mountains led to recognize four different
sedimentary units forming distinct cycles bounded byunconformities.
The first one is represented by "Trubi" Formation,

54==========================

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

consisting ofmarls and marly limestones, which range fromzone MNN12 (Rio et al., 1990) to zone MNN14/15 (Early
Pliocene).
The second one consists of clays, sands and calcarenites ranging from the upper part of zone MNN14/15 to
MNN16a/17 (Early-Middle Pliocene).
The third is made up by sands and calcarenites assigned
to the zones MNN19a and MNN 19b (Late Pliocene-Early
Pleistocene).
The fourth represented mostly by clays, belongs to thezones MNN19e and MNN 19f (Early-Middle Pleistocene).
Deposition of the Plio-Pleistocene sequences by eustatic
fluctuations and the tectonic history of the Tyrrhenian Sea
opening.
REFERENCES
Rio D. Raffi I. and Villa G., 1990: Pliocene-Pleistocene
calcareous nannofossil distribution patterns in thewestern Mediterranean. Proc. ODP, Sci. Res., 107,513-533

PALEOECOLOGY OF mE PALEOCENE NANNOPLANKTON
0/ga B. Dmitrenko
Topics: Cenozoic Atlantic/Indian oceans, Paleoecolon

In the basis of this paper lays the vast quantity of data
about calcareous nannofossils presence, distribution andabundance in the bottom sediments of the Atlantic and theIndian oceans. These sediments were sampled during deepsea drilling by "Glomar Challenger" and "Djoides
Resolution". The paleoecology study includes: the analysisof the distribution of different species and groups of species
by area; the change of common nannoplankton abundancewith time; the change of the individual species abundance;
the perculiorities of the most numerous species variations.
All of this gave the opportunity to make more precise thepaleoecology of different species and to distinguish thenannofossil' s groups of the different paleogeographic
environments. The data about more than 300 species wasused. More than 500 areal-ranges were constructed for 9
moments from 65 to 25 Ma ago during 5 Ma. On the basisof these areal-ranges the profiles of the different species'
distribution and the abundant changes after changes ofthe latitudes were constructed.

The partly-quantity data from the volumes of the DSDP
and ODP was used. The common nannoplankton
abundance and the changes of the common coccolith'smasses were taken into account for the construction of themeridional profiles, and were traced along the time. The
analysis of all of these materials allowed to distinguish all
the paleogene species in the few paleoecologic groups:
1. Equatorial-tropic species, with no markableconcentration;
2. The narrow-tropical species, those that form and that
do not form the high concentrations;3. The species of the broad geographic distribution withincreasing of the concentrations in the tropicalenvironments;
4. Subtropical species of the general and bipolar
distributions;5. The species of the cold subtropics and moderate areas.
There have high concentrations, and their distribution canbe wide or bipolar.

CALCAREOUS NANNOFOSSILS AS PALEOPRODUCTIVI1Y INDICATORS IN
CAMPANIAN- MAASTRICHTIAN UPWELLING SYSTEMS
Yoram Eshet and Ahuva Almogi-Labin
Tuesday, 12.25
During Santonian to Maastrichtian times, enhanced
upwelling conditions prevailed along the southern marginof the Tethys, resulting in the accumulation of thick sectionsof organic-rich cartxmates, phosphates and cherts. In order
to contribute to the understanding of the ecological andoceanographic conditions in this system, the calcareous
nannofossil assemblages from Campanian-Maastrichtianorganic-rich cored sections in the subsurface of Israel wereanalyzed. Previous micropaleontological studies(forarninifera, dinoflagellates) and geochemical studies
showed that the sedimentation of these sequences wascontrolled by the interplay between surface waterproductivity and bottom conditions. Calcareous
nannofossils from 150 samples in these sections wereanalyzed in the present study in order to identify taxa thatcan be used as indicators of productivity, and taxa whose
degree of preservation reflects bottom conditions. The
following results were obtained:===========================55

1. Nannofossil assemblages abundance and species
diversity decrease in high productivity conditions. On theother hand, in lower productivity and open marine
conditions, assemblages reach the highest abundance anddiversity. Similar trends are reported from peridinioid
dinoflagellates that become abundant in high productivity,and from gonyaulacoid dinoflagellates that increase in lower
productivity conditions (P /G ratio).
2. Micula decussata was found to be a good indicatorof preservation; in badly- presetved samples, its abundance
increases drastically. This result is supported by previous
experiments that showed the dissolution-resistance ofthis
taxon. On the other hand, the distribution of Watznaeueria
barnesae, another reported-to-be dissolution-resistanttaxon doesn't always match well with the presetvation curve
obtained for the studied sections: in some intervals its
distribution seems to be affected by productivity.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA-Conference, Copenhagen 1995, Programme and Abstracts.

3. Based on matching their distribution curves withproductivity reconstruction curves offered by planktic
foraminifera and dinoflagellates, higher amounts of sometaxa were found to reflect lower productivity conditions:Thorachosphaera opercu/ata, Lithraphidites carnio/ensis, Vekshine//a spp., Prediscosphaera spp. andEiffe/ithus turriseiffelii. The highest productivity intervals are represented by higher abundance of G/auko/ithus
spp., Biscutum spp. and Thorachosphaera saxea.
4. The nannofossil index of productivity, as suggested
in this study, is useful in reconstructing paleoproductivity
history, and matches well with reconstructions made byother micropaleontological disciplines.

CALCAREOUS NANNOFOSSIL DATUM LEVELS: A KEY FOR THE
UNDERSTANDING OF THE GENESIS OF UPPER CRETACEOUS OIL SHALE
SECTIONS IN ISRAEL
Eshet, Y., Minster, T., Moshkovitz, S.
Poster session
Chalks and marly chalks enriched in organic matter (oilshales) are abundant in the Maastrichtian sequence ofIsrael, especially in synclinal structures. In order tocontribute to the understanding of oil shale basin
development, Maastrichtian calcareous nannofossil datum
levels were determined in selected boreholes thatpenetrated the oil shale 'facies' of the Ghareb Formation in
the Rotem Syncline, northern Negev. The studied
boreholes form longitudinal and latitudinal seetions acrossthe Rotem syncline.
The following calcareous nannofossil datum lines were
determined (absolute ages are quoted from the literature):-Last occurrence of Quadrum trifidum (73 MA).
-Last occurrence of Reinhardtites /evis (71.5 MA).
-First occurrence of Lithraphidites quadratus (70 MA).
The results shed new light on some aspects of thedevelopment of the basin during the oil shale formationand may be used for better understanding of thesedimentary and tectonic evolution of the basin during
the time period represented by the oil shale sequence:
1. The top of the oil shale unit demonstrates a sharp
diachronic nature - in the southern part of the basin it
appears close to and below the first occurrence of L.

quadratus, whereas in the north it is found in much older
layers, below the last occurrence of Q. trifidum.
2. Based on the absolute ages of the determined datum
lines and on the assumption that the base of the oil shale
unit (base of the Ghareb Fm.) is almost of equal time, itappears that the oil shale unit does not represent equal
time-spans all over the syncline; in its northern part, it
represents a period of about 1-1.5 MA, whereas in the south
it represents a much longer time interval, up to 4-4.5 MA.
3. The sedimentation rates which were computed forthe oil shale sequence in the Rotem syncline vary between
15-40 m/MA. The highest rates were attained in the central
and southern parts of the basin, whereas towards the north,lower rates were recorded.
4. The nannofossil datum lines indicate the existence ofa major depo-centre, that developed mainly after the last
occurrence of Q. trifidum, in the central to southern part ofthe oil shale body. A NNW-SSE trending hinge line, passing
through the joining point of the Havarbar-Ef'e valleys wasdeveloped during that period and generated two subbasins: a northern, smaller, and a southern, a larger one. A
gentle, differential uplifting of the eastern flank of the basin
during the same period is also indicated by the nannofossil
datum levels.

CALCAREOUS NANNOFOSSIL BIOSTRA TIGRAPHY IN SANTONIANMAASTRICHTIAN ORGANIC- RICH CARBONATE SECTIONS IN ISRAEL
Y. Eshet, and S. Moshkovitz
Poster session
A calcareous nannofossil zonation scheme is presented for
Santonian-Maastrichtian organic-rich carbonate sequencesin southern and central Israel, that were deposited in astrong upwelling system along the southeastern Tethys.
The zonation is correlated with foraminifera and organicwalled dinoflagellate cyst zonal schemes for the same
sequences. The following zones are recognized:- Lucianorhabdus cayeuxii Zone, Sissingh, 1977 (Late
Santonian)-NC 16- Aspido/ithus parcus Zone, Verbeek, 1976 (Early
Campanian)- NC 18- Ceratolithoides acu/eus Zone, (Cepek and Hay, 1969)
Martini, 1976 OateEarly Campanian)- NC 19a- Quadrum sissinghii Zone (Sissingh, 1977) PerchNielsen, 1985 (early Late Campanian)- NC 19b- Quadrum trifidum Zone, Bukry and Brarnlette, 1970
(Late Campanian-Early Maastrichtian)- NC 20- Arkhangelskie//a cymbiformis Zone, (Perch-Nielsen,1972)Mart.ini, 1976 (Early-MiddleMaastrichtian)subzoneA- NC 21a
subzoneB-NC21b- Lithraphidites quadratus Zone, (Cepek and Hay,
1969) Bukry and Bramlette, 1970 (Middle Maastrichtian toearly Late Maastrichtian)- NC 22
In this study we suggest that the NC21 Zone (according
to Monechi and Thierstein, 1985) is subdivided into two
subzones: NC21aandNC21b. Wealsonotethatsometaxa
that are commonly used as markers elsewhere, have a
different range in the studied area.

56============================

...

6th INA Conference, Copenhagen 1995, Programme and Abstracts .

The proposed zonal scheme indicates the occurrenceof unconformities at the Santonian-Campanian boundary
and within the upper part ofthe Middle Maastrichtian.
Calculations of sedimentation rates indicate anincreasing mte towards the north, and that there is a general..

Journal of Nannoplankton Research, 17, 2, 1995.

trend of rate increase through time from the Santonian to
the Maastrichtian. A significant rate increase is found insections from the outer shelf and continental slope at thefirst occurrence of Quadrum sissinghii and Quadrum

trifidum.

CALCAREOUS NANNOPLANKTON FROM THE AUSTRALIAN SECTOR OF THE
SOUTHERN OCEAN
C/aire Find/ay_
Poster session
Calcareous nannoplankton assemblages were recorded fromwater column samples between 1Om and 200m water depth,
from the Australian Sector of the Southern Ocean. Samples
were taken during the summer months from December 1993
to January 1994, between 48°19'S and 64°09'S, and143°52'E (WOCE-V7 cruise), and from January to February,
1995, between 41°00'26"S and 49°04'S, and between
142°3l'E and 151°22'E (Australian Geological Survey
Organisation cruise 14 7).
Particular attention was given to Emiliania huxleyi,
and various measurements were recorded and compared toprevious studies (Young and Westbroek, 1991 ). The results
show the most dominant morphotype of E. huxleyi fromthe WOCE-V7 samples compares to Type C of Young andWestbroek, the 'cold water' form (though the morphotypes
are not necessarily influenced solely by temperature)described by previous workers (Mclntyre and Be, 1967;
Okada and Honjo, 1973). The 'polar form' described by
Verbeek ( 1989) was also present. Biogeographic plots ofE.
huxleyi from these samples show a change in abundanceand diversity at depth (90 to 1OOm), and latitude.
Ca/cidiscus leptoporus, the second major component in
the WOCE-V7 transect, is absent south of 49°45'S,
indicating the position of the Subtropical Convergence(Subantarctic Front), and the absence of E. huxleyi southof 61°20' S indicates the position of the Polar Front(Antarctic Divergence). Gephyrocapsa species were notfound in the WOCE-V7 samples
Initial investigations of the AGSO samples indicate avery different assemblage between the two transects. The

dominant form in the north of this transect is
Umbel/osphaera tenuis, not the expected 'warm water'
form of E. huxleyi. This indicates a different water masscompared to the west ofTasmania and possibly reflects thepresence of southward-flowing, warm-water, near-coastal
currents, such as the Leeuwin and Zeehan Currents.
Although Gephyrocapsa oceanica is present, it is not asignificant component of the assemblage.
Comparison with temperature and salinity data for thisregion should determine the different water masses andhow they affect the composition of calcareous
nannoplankton assemblages in this section of the Southern
Ocean. This information will be compared with downcore
assemblages to determine the changes in the Southern
Ocean through the Quaternary.

REFERENCES
Mclntyre, A. and Be, A.W.H., 1967: Modern
coccolithophoridae of the Atlantic Ocean-!. Placoliths
and Cyrtoliths. Deep Sea Research, 14: 561-597.
Okada, H. and Honjo, S., 1973: The distribution of oceanic
cocco-lithophorids in the Pacific. Deep Sea Research,
20: 355-374.
Verbeek, J.W., 1989: Recent calcareous nannoplankton
in the southernmost Atlantic. Polarforschung, 59(112):45-60.
Young, J.R. and Westbroek, P., 1991: Genotypic variationin the coccolithophorid species Emiliania huxleyi.
Marine Micropaleontology, 18: 5-23.

MAASTRICHTIAN NANNOFOSSIL BIOGEOGRAPHY IN THE
SOUTHERN TETHYS
Andrea Fiorentino
Wednesday, 11.10
Nannofossil assemblages from Southern Tethys sections
were analyzed in order to identify patterns of geographic
distribution arid their causes. The general biogeographic
scheme for this period of time was difficult to apply, due tothe changes in the composition of the assemblages observed
locally. The geographic distribution of selected nannofossil
species was therefore interpreted in another perspective,
considering the influence of the environment of deposition,=========================57

the lithology, the effects of preservation and the geologic
history of the sections examined. The absences of Micula
decussata and Braarudosphaera bige/owii fromassemblages, of which they should be typicalrepresentatives, are reported and a tentative explanation is
given, suggesting that geographic distribution of a species
is strongly affected by factors other than only temperatureand latitude.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

AN EXAMPLE OF EUTROPHIC-OLIGOTROPHIC ALTERNATES IN mE LOWERMESSINIAN: THE SORBAS BASIN (WESTERN MEDITERRANEAN)
JA . Flares, FJ Sierra, I. Zamarreno, A. Vazquez, R. Utri//a and G. Frances
Poster session
In the Sorbas section (Lower Messinian, SE Spain), thecalcareous plankton microfossils assemblages show acyclicity interpreted as precessional orbital forcing, as effectof changes in the surficial water characteristics. Here, adetailed analysis of the calcareous nannofossils (CN)assemblages in three cycles is carry out, using quantitativetechniques. The lithology of these cycles consist of hard(partially silicified and calcareous nannofossil sterile) levels,
separating two meters marly levels very rich in calcareousplankton. The proportions of the Planktic Foraminifera (PF)warm assemblages show the same distribution that
Asteroliths and Sphenoliths, richest in the lower part of themarls levels. However, the Sphenolith peak preceeds theAsterolith peak. The frequencies of the Very Small
Reticulofenestrids (VSR; most important group in the CN
assemblages) are opposite to those of Asteroliths andSphenoliths, increasing towards the top ofeach marly cycle.
Using the Scanning Electro Microscope in not disturbed
samples, is observed that the VSR richest intervals are theless diluted and richest in complete coccospheres. It is
discussed the possibility that these VSR dominant levels
correspond to maximum eutrophic episodes. On thecontrary, the Asterolith-Sphenolith rich assemblages should
correspond to oligotrophic episodes in the basin. Thisdinarnic is related to variations between the Sorbas and theMediterranean connection during the Messinian.

BIOSTRA TIGRAPHY USING SILICOFLAGELLATES AND CALCAREOUS
NANNOFOSSILS OF NEOGENE- PLEISTOCENE DEPOSITS OF GREECE
Patras Dimitris Frydas
Monday, 16.00

An intensive research using calcareous and siliceous
nannofossils has been carried out in the South AegeanSea, Greece. New subzones of the siliceous nannofossils
were identified and correlated with stratigraphicallyequivalent planktonic foraminiferal and calcareous
nannoplankton zones.
A continuous sedimentation from Tortonian to Lower
Piacenzian is observed in the Neogene deposits of Creteisland, with a thickness of more than 500m During the Upper
Miocene a rhythmic alternation of thick evaporite beds
with gypsum (Selenit), sandstones and larninateddiatornite
layers was deposited. The Pliocene succession mainly
consists of grey silty clays, yellow marls and light grey towhite diatomites or diatornaceous marls.
From a total of nine formations which have beenrecognized from the East to the West of Crete island, threewere deposited during the Upper Miocene and the rest
during the Pliocene.
The silicoflagellates of the Kavoussi section, W. Creteare placed to the interval-Zone Distephanus speculum
minutus. The latter is equivalent to the CN9 (Discoaster
quinqueramus) characterized by the DisccX1ster berggrenii
and the D. quinqueramus first occurrences (Upper
Miocene).
The Pyrgos, Dafnes, Tsagaraki and Makria Rachi
sections situated at the central part of Heraklion district,Crete, can be assigned to the Dictyocha aspera aspera
Acme-subzone, which is considered stratigraphicallyequivalent to the CN9b (Amaurolithus primus) subzcme of
the Messinian. Similarly, the Ragani section association,
NW Corf'u, belongs to the same subzone (D. aspera aspera),
which is also equivalent to the Globorotalia conomiozea
Zone of planktonic forarninifera.
Using the silicoflagellate percentage distribution, theLower Piacenzian has been subdivided into four new
subzones, listed below (from older to younger): theDictyocha brevispina brevispina Acme-subzone, theDictyocha neonautica Acme-subzone, the Cannopilus
major Acme-subzone, and the Distephanus boliviensis
Acme-subzone. These subzones are coeval to the CN12a(Discoaster lama/is) subzone as well to the G/oborotalia
bononiensis Zone.
The silicoflagellates associations from the section Frago(Milos island) as well Aghios Thomas ( Aegine island) wereplaced in the Acme-Zone Mesocena circulus (Upper
Zanclean). The calcareous nannofossils from both sections
indicate the biozone CNllb (Discoaster asymmetricus)
through the coexistence of Discoaster tamalis andReticu/ofenestra pseudoumbilicus. This biozone
corresponds to the zone of Globorotalia puncticulata fromplanktonic foraminifera. Further the silicoflagellate
association of the section SE-Adamas (Milos island)
belongs to the Acme-subzone Octactis pulchra (Lower
Pleistocene) which corresponds to the zone CN13a(Emiliania annula) from calcareous nannoplankton.

58========================~

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

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EARLY CRETACEOUS CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF
THE INTERNAL LIGURIDS (NORTHERN APENNINES, ITALY) AND THE ONSET
OF COCCOLITH- BEARING SEDIMENTS IN THE LIGURIAN- PIEDMONTOCEANIC DOMAIN
Si/via Gardin and Nico/a Perilli
Poster session
Topics: Biostratigraphy, Early Cretaceous, Western Tethys, Northern Apennines, Italy.

The internalligurid succession of the Northern Apennines(Italy) consists of Early to Middle Jurassic ophiolite

sequences, interpreted as slabs of the Western Tethys

oceanic lithosphere, and their pelagic sedimentary cover(Principi et alii, 1992 and reference therein). The Middle
Jurassic-Early Cretaceous pelagic cover includes radiolaritic========================59======================~

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

sediments, as the Mt. Alpe Chert, and coccolith-bearing
formations as theNisportinoFm., the CalpionellaLimestone
and the Palombini Shale.
During the Callovian-Tithonian time interval the oceanic
Ligurian-Piedmont basin, located between Europe and Adria
continental margins, was interested by the sedimentationof well-stratified ribbon radiolarites (Mt. Alpe Chert:
Baurngartner, 1984; Marcucci and Conti, 1986). In the
Berriasian the siliceous sedimentation passed to the siltymarly deposition of the Nisportino Fm. (Bortolotti et alii,1994) and/or to the calcareous sedimentation of the
Calpionella Limestone. The Calpionella Limestone, madeup of siliceous and marly limestones, it is overlain by the
Palombini Shale, which consist of marlstones, marlyclaystones and siliceous or marly limestones (Perilli, 1995;
Perilli and Nannini, 1995 and references therein).
This work deals with calcareous nannofossil
biostratigraphy of the Early Cretaceous sedimentation ofWestern Tethys and the onset of coccolith-bearing
sediments in the Ligurian-Piedmont oceanic basin; thisstudy contribute to lighten the sedimentary evolution of
the Ligurian-Piedmontese oceanic domain.
The hernipelagic deposition of the Nisportino Fm.
started in the early Berriasian; the pelagic sedimentation of
the Calpionella Limestone took place within the late
Berriasian. During the early to late Valanginian the
Calpionella Limestone sedimentation gave way to thedeposition of the Palombini Shale, which was ubiquitousin the whole Ligurian-Piedmont basin until the early

the presence of very similar forms (Rucinolithus cf. R.
terebrodentarius) even from the Retecapsa angustiforata
biozone.
The studied nannofossil assemblages of theinvestigated sections, which belong to an oceanic domain,
reveals remarkable differences in composition and total andrelative abundance of species compared with other of sameage but belonging to different epicontinental
paleogeographic setting (e.g Southern Alps: Erba andQuadrio, 1987; Umbria-Marche basin: Braloweret al., 1989;
Vocontian basin: Gardin and Manivit, 1993). These
differences, partly due to the lithology and preservation,
are also related to paleoproductivity and paleogeography.

Barremian
The recognized biozones (following Thierstein 1971,
1973, 1976) are: Nannoconus co/omi Zone: this easily
recognizable biozone is characterised by the sharply
increase of the genus Nannoconus with specimens larger
than 8J-Lm and the first occurrence of Nannoconus
steinmannii steinmannii togheter with Nannoconus
kamptneri; the zonal marker is occasionally present withrare specimens. Retecapsa angustiforata Zone: besides
the zonal marker Retecapsa angustiforata, which is present
even if with rare specimens, this Zone is characterised by
the FO of Rucinolithus wisei, the FO of Percivalia
fenestra fa, the FO of Tubodiscus jurapelagicus, and theFO of Tubodiscus verenae. Within this Zone we recorded
the presence of Rucinolithus cf. R. terebrodentarius and,in the upper part of the Zone, of Calcicalathina aff.
Calcica/athina oblongata, a precursory form ofCalcicalathina oblongata. Calcicalathina oblongata
Zone: as reported by many authors, this is an interval inwhich there are few appearances or extinctions of common
species and therefore, it is difficult to finely subdivide it.
Rucinolithus wisei and Tubodiscus verenae sporadicallyoccur and get extinct in this biozone, although their LO' s is
not clearly detectable. Within this biozone it is also
recorded the FO of Nannoconus bucheri (and wide canalrelated forms), but this event needs to be further tested.
Litraphidites bollii Zone: The difficulty in characterising
this Zone is the lack of the zonal marker Litraphidites bollii
in the studied deep-sea lithofacies; however, within thisbiozone the LO of Cruciellipsis cuvil/ieri is easily welldetectable; on the contrary the FO of Rucinolithus
terebrodentarius is questionable due to, as above reported,

REFERENCES

Baumgartner P., (1984) -A middle Jurassic-early Cretaceous low latitude Radiolarian zonation based on
Unitary Association and age of Tethyan Radiolarites.
Eclogae geol. Helv. 77,729-837.
Bortolotti V., Gardin S., Marcucci M. and Principi G.,(1994) - The Nisportino Formation: a transitional
unit between the Mt. Alpe Cherts and the Calpionella Limestone, Elba Island. Ofioliti sp. issue (in press).
Bralower T. J., Monechi S. and Thierstein H. R., (1989)Calcareous Nannofossil Zonation of the JurassicCretaceous Boundary Interval and correlation
with the Geomagnetic Polarity Timescale. Mar.
Micropal., 14, pp. 153-235.
Conti M. and Marcucci M., (1986) - The onset ofradiolarian deposition in the ophiolithes sequence of
the Northern Apennines. Mar. Micropal., 11, 129-138.
Erba E. and Quadrio B, (1987) - Biostratigrafia a Nannofossili calcarei, Calpionellidi e Foraminiferi planctonici
della Maiolica (Titoniano superiore-Aptiano) nelle
Prealpi Bresciane (Italia settentrionale). Riv. Ital.
Paleont. Strat., 93,3-108.
Gardin S. and Manivit H., (1993) - Upper Tithonianand Berriasian calcareous nannofossils from the
Vocontian Trough (SE France): biostratigraphy andsequence stratigraphy. Bull. Rech. Explor.-Prod. Elf
Aquitaine, 17,277-289.
Perilli N., (1995) - Lower Cretaceous nannofossil
biostratigraphy of Calpionella Limestone and Palombini
Shale (Ligurian Formation) in South.ern Tuscany.
Submitted to Revista Espagnola de Paleontologia.
Perilli N. and Nannini D., (1995). Calcareous
nannofossil biostratigraphy of the Calpionella
Limestone and Pa1ombini Shale (Bracco Val Graveglia
Unit) in the middle Val di Vara (eastern Liguria, Northern
Apennines). Submitted to Ofioliti.
Principi G., Cortesogno L., Cellai D., Gaggero L., Garuti G.,
Gazotti M., Passerini P. and Treves B., (1992) B 1: Le ofioliti dell' Appennino settentrionale. 76
Riunione estiva SGI, Guida all'escursioni Post
Congresso, pp. 1-76. Firenze 21-23 Settembre 1992.
Thierstein H. R., (1971)·- Tentative Lower Cretaceous
calcareous nannoplankton zonation. Eclogae geol.
Helv., 64, pp. 459-488.
Thierstein H. R., (1973)- Lower Cretaceous calcareous nannoplankton biostratigraphy. Abh. geol. Budens., pp. 1-52.
Thierstein H. R., (1976) - Mesozoic calcareous
nannoplankton biostratigraphy of marine sediments.
Mar. Micropal., I, pp. 325-362.

6o========================~

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995.

SEDIMENT TRAP STUDIES OF COCCOLITH AND PLANKTONICFORAMINIFERAL FLUXES IN THE BENGUELA UPWELLING SYSTEM
Jacques Giraudeau and Geo.ffrey W Bailey
Monday, 16.50

Coccoliths and planktonic foraminifera collected by asediment trap deployed on the upper slope offWalvis Bay,
Namibia, were investigated in order (1) to assess theircontribution to the total particulate flux, (2) to evaluate
their response·to seasonal changes in the dynamics of the
Benguela upwelling process, and (3) to use them as tracersof particle transfer process on the slope. The trap, locatedat 545 m depth, 50 m above the sea floor, provided highresolution (8 days) times series samples from late winter toearly summer. This 4-month period is marked by a drasticchange in hydrological processes, from active to quiescent
upwelling conditions. The total mass flux ranged from 3 to
1, lg/m 2 /day. The lithogenic fraction was the main
contributor to the total mass flux (64% of averagecontribution), followed by carbonate (22%), organic matter(8%), and biogenic opal (5%). The relative contributionsof the four components to the total mass flux were relatively
stable throughout the period of the experiment, thereby
suggesting that seasonal changes in hydrological/upwelling
process, from late winter to early summer, did not induce
sharp modifications in the composition of the particles
sedimenting on the slope. The bulk oflithogenic particles
sedimenting on the continental margin originates fromaerosol sand plumes due to katabatic wind events.
Considering the low frequency and short duration of such
events, we suggest that resuspension of shelf material andcontinuous horizontal advection to the slope werenecessary to account for the high contribution oflithogenic
particles recovered by our trap throughout its 4-monthdeployement.
The free-coccolith mass flux closely followed total massflux variations, and ranged from 90 to 10 mg/m2 /day, thereby
accounting for less than 10% (on an average) of the total
biogenic carbonate mass flux. Coccolith number fluxes
varied from 4200 106/m2/day to 400 106/m2 /day, Emiliania
huxleyi being the dominant form (relative abundance: 60
to 75%) . On the contrary to coccolith fluxes, thecoccosphere fluxes did not show any significant
covariations with total mass fluxes. This, coupled, with
dissimilarities in species assemblages, suggest that the bulk
coccolith fraction and the coccospheres were affected by
distinct transfer process: lateral transport of coccoliths
resuspended from the shelf, vertical advection of
coccospheres from the overlying surface waters.
Planktonic foraminiferal number fluxes, dominated byjuvenile specimens, ranged from 600 to 50 103 1m2 /day, androughly followed the total mass flux variations. The threesize classes (juvenile, neanic, adult) presented distinct
patterns in flux variations, which can be related to distinct
transfer process, as well as mass mortality events in thecase of the adult populations.

OCEANIC FRONTS IN THE MESOZOIC
William W Hay
Poster session

The modem ocean is characterized by four regions, threeof which are mirrored in each hemisphere: an equatorial
belt (28% of the ocean surface area) characterized bydivergence and shared by the two hemispheres, stratified
tropical-subtropical anticyclonic gyres (46%), temperate
mid-latitude belts of water characterized by convergenceand steep meridional temperature gradients (11%), anddeeply convecting polar oceans characterized by cyclonic
gyres (13%). Convergence and divergence of the ocean
waters are forced beneath zonal winds. Convergences orfronts form sharp boundaries between water masses andintroduce surface water into the ocean interior. The fronts
can be recognized by abrupt changes in nannoplankton
assemblages. The sites of divergence are more diffuse; they
separate water masses and return water from the oceaninterior to the surface. Surface waters of the equatorial belt
flow westward, driven by the easterly trade winds. Eastward
subsurface flow returns some of the water, but much of the
westward flow becomes incorporated into the westernboundary currents of the tropical subtropical gyres.
Increasing zonal velocities of the trade winds away fromthe atmospheric Intertropical Convergence Zone (ITCZ)===========================61

induce divergence and upwelling in the waters of theequatorial belt. The most stable features of the modem
ocean are the stratified tropical-subtropical gyres between
15° and 45° Nand S. Low-latitude easterly trade winds andmid-latitude westerly winds drive the gyres. They also force
convergence in the gyre centres. The sinking waters spreadbeneath the gyre as central waters. The maximum of thezonal component of the westerly winds occurs at about 45°
N and S. The zonal winds induce meridional flow of thesurface waters toward the equator, forcing sinking along
the subtropical and polar fronts and forming barriers topoleward heat transport. The subtropical front is the source
ofthermocline water. Intermediate water forms by sinking
along the polar front. The alternate, competing, source forintermediate water is outflow from saline marginal seas.
Decreasing zonal wind velocities poleward of the polar
fronts induce divergence, cause cyclonic circulation, andpromote deep convection and deep water formation.
The Jurassic and Early Cretaceous ocean may havebeen similar to that of the present, but the late Cretaceous
ocean was significantly different, with polar temperatures
well above 5° C. The tropical-subtropical gyres in theJournal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Panthalassic Ocean had high salinities, though not as highas in the early Atlantic. Central waters would have formed
as they do todi.y. The subtropical and polar fronts, driven
by the winds, must have existed, and would have been
located in the mid latitudes even if the poles were warmer
than today. Between the subtropical and polar fronts boththe temperature and salinity of the water must havedecreased, representing the outcrop of the lower part of
the tropical-subtropical pycnocline. Nannoplankton
assemblages indicate that the subtropical fronts in the
Cretaceous were at the same latitude as they are today.
The Cretaceous term for the region equatorward of thesubtropical fronts is "Tethyan," the regions poleward are"Boreal" and "Austral."

CALCDINOCYSTS FROM THE MIDDLE CONIACIAN TO UPPER SANTONIANCHALKS AT LAEGERDORF (N GERMANY)
Tania Hi/debrand-Habe/ and Helmuth Wi//ems
Poster session
Calcareous dinoflagellate cysts are a very common, often
even rock-forming nannofossil group in the pelagic chalkfacies of northern Europe. According to the systematicconcept ofKEUPP (1987) and KOHRING (1993), fourmorphological groups of cysts within the Calciodinellaceae
DEFLANDRE 1947 can be distinguished on the level ofsubfamilies. l'he striking feature is the orientation of thecrystallographic c-axis of the calcite crystals in the outercyst wal L _relati-ve- -to - -the cyst surface . The
Orthopithonelloideae are characterized by an orthogonal(radial), the Obliquipithonelloideae by an irregularly
oblique, the Pithonelloideae by an uniquely oblique, andthe Fuettererelloideae by a tangential orientation of thecrystals. From the 400 m thick Upper Cretaceous white chalkstandard section ofLaegerdorf- Kronsmoor (N Germany),a first survey of calcareous dinocyst assemblage is given
for the time period of middle Coniacian to upper Santonian.
24 samples have been studied from the 85 m thick series
from the koeneni Zone to the Uintacrinuslgranulata Zone.
The spectrum offorms comprises 27 taxa, three of them aredescribed newly. In addition to the systematic description,
the flora has been interpreted paleoecologically using
quantitative evaluations. Summarizing representations of
the distribution of the subfamilies and further
morphological groups, of the diversity, and of the frequency
have been established on the basis of vertical cyst
distributions. The tendencies to be derived from thesepatterns allow a rough division of the section into threestratigraphic ranges. Considering the studies of otherauthors, the distributions seem to be related to transgressive/
regressive trends. Possibly, the lower range of the section(koeneni Zone) indicates a regressive trend, the middle range(upper middle Coniacian to lower middle Santonian) atransgressive trend, and the upper range (middle Santonian
to upper Santonian) a regressive trend.
REFERENCES

Keupp, H.(l987), Facies, 16: 37- 88; Erlangen.
Kohring, R. (1993), Berliner geowiss. Abh.(E), 6: 1 - 164;
Berlin.

UPWELLING RELATED DINOFLAGELLATE CYST ASSOCIATIONS OF
THE BENGUELA CURRENT SYSTEM
Ramses P. Hoek and Karin A.F Zonneveld
Poster session
Dinoflagellate cysts are recorded from most marine
environments and are susceptible to changes intemperature, nutrients and salinity. Little is known,
however, of the environmental affinity of dinoflagellate
cysts from subtropical regions of the Atlantic Ocean.
The Benguela Current System, the eastern boundary
current of the South Atlantic subtropical gyre, can be
subdivided into a northward-directed, relatively cold, nearcoastal upwelling part and a relatively warmer north tonorthwest flowing oceanic part.
Surface sediments ofboth multicores and boxcores fromthe Benguela Current System are studied for theirpalynologic content, with emphasis on organic-walled
dinoflagellate cysts (dinocysts). Preliminary results, related
to known oceanographic parameters, will be presented here.
Dinoflagellates producing organic walled cysts may
have heterotrophic and/or autotrophic (photosynthetic)

feeding strategies. The associations recorded in the samples
from the main upwelling cell (Walvis Bay) are dominatedby heterotrophic, dinoflagellate cysts (representatives ofthe family Peridiniacea) with a total of 12000 dinoflagellate
cysts per cm3 • Several of these species seem to be endemic
for upwelling areas and are only recorded in large
concentrations in studies offshore Somalia and Peru.
Concentrations are relatively lower in and close to the
freshwater plume of the Orange river. An increase in theamount of terrestrial derived material (pollen, spores andfresh water algae) is observed here.
Concentrations of dinocysts decrease oceanward (289000 dinocysts per cm3), and are primarily concomitant withan increase in the relative amount of autotrophic
dinoflagellate cysts (representatives of the family
Gonyaulacaceae).

62========================~

Journal of Nannoplankton Rese!lrch, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

CORRELATION OF CALCAREOUS AND ORGANIC- WALLED DINOFLAGELLATECYST ASSOCIATIONS IN GLACIAL/INTERGLACIAL CYCLES, AN EXAMPLE
OF THE EQUATORIAL ATLANTIC
Christine Hoe//

Poster session
Organic-walled dinoflagellate cysts (organic dinocysts)
have been described from sediments of almost all marine
environments, whereas calcareous dinocysts often havebeen neglected. The occurrence of organic dinocysts ismostly restricted to neritic regions only a few species livein the oceanic reabn. On the contrary, calcareous dinocysts
occur mostly in oceanic regions and less in neritic. One
sediment core (from the Guinea Basin, Equatorial
Divergence Zone of the South Equatorial Current, Core
GeoB 1105-4) was used for the investigation for both,
calcareous and organic dinocysts. Most of the organic
dinocysts are formed by gonyaulacoid, autotrophic
dinoflagellates or protoperidinoid, heterotrophic
dinoflagellates. Among the calcareous dinoflagellates, it
has to be differentiated between calcareous dinoflagellate

cysts (calcareous dinocysts) and the vegetative coccoid
form Thoracosphaera heimii. The analysis of the dinocysts
assemblage shows a much greater amount of calcareous
forms, which are mainly dominated by the vegetative
coccoid form ofT. heimii. The total cyst flux of organic
dinocysts increases during glacial periods together with apredominance of protoperidinoid cysts. The predominanceof these cysts can be related to higher nutrient levels and/or a decrease in temperature. The amount of calcareous
dinoflagellates including T. heimii is especially high at the
beginning of glacial periods. Assemblages of organic
dinocysts and calcareous forms both show striking changes
in composition and flux from glacial to interglacial. The
vegetative form T. heimii seems to be a valuable directindicator for paleoproductivity.

MID- CRETACEOUS CALCAREOUS NANNOPLANKTON IN AN ORGANIC- RICH
FACIES OF THE SUBBETIC AND PENffiETIC (BETIC CORDILLERA,
SOUffiERN SPAIN)
Glen Homeier

Poster session
Calcareous nannoplankton and Rock-Eval analyses ofCo _rich intervals are used as tools to provide a bett~understanding of the mid-Cretaceous paleoceanographic
conditions around the Alboran-microcontinent in southern
Spain. Ten sections and ten high-resolution profiles(sampled in cm intervals) are being investigated along theaxis (Median-Subbetic) and at the margin (Penibetic/
Internal-Subbetic) of the "Betic Seaway". Nannofossil andorganic carbon data are compared with "Oceanic Anoxic
Events" (OAEs) within deep sea drilling sites (DSDPI ODP)of the North Atlantic Ocean.
Pelagic (Barremian)-Aptian-Aibian (OAE-1) darkmarlstones/claystones, marly lime-stones and black shales(> 1% TOC) were mainly investigated in the Sierra de las
Cabras in the western Subbetic and the Sierra de Ios
Canutos (Manilva) in the Penibetic. Calcareous Nannofloras
are poorly preserved but are common in black shales with
Total Organic Carbon (TOC) contents up to 3% during theAptian. The Albian deep-marine sediments of the MedianSubbetic consist of alternating dark green, bioturbatedclaystones, grey claystones and black shales. Benthic
foraminiferal assemblages indicate deposition below thecalcite composition depth (CCD) in the Rio Fardes area
(Central-Subbetic) (Homeier, 1993; Reicerteretal., 1994).
Calcareous nannoplankton and planktonic foraminifera areabsent and C -values reach up to 2,6% TOC. The kerogenis of type-Ill ~rding to the Rock-Eval data and contains
terrestrial macerals (fusinite, sporenite, vitrinite). Further
to the Northeast, in the Sierra de Ponce area (East-Subbetic)
calcareous nannoplankton is relatively abundant in thedark claystones (0,7% TOC). This implies that this Subbasinof the Median-Subbetic was located above the CCD incontrast to the sub-CCD conditions in the Rio Fardes-Basin.
Black shale~; at the Cenomanian/ Turonian boundary=========================63(OAE-2) reach 16,7% TOC in the Rio Fardes area (Homeier,
1993; Section Olivares). They are intercalated with finegrained calciturbidites, grey marlstones and calcilutites withblack banded chert, rich in radiolarians. This is a typicalfacies association of the Cenomanian-Turonian Boundary
Event (CTBE) in the entire Subbetic. Calcareous
nannoplankton is rare and occurs mainly in the interstratified
horizons between the black shale layers. They show low
diversity and poor preservation. Most of the species areintensively overgrown and dissolution is present. The
dissolution resistant species Watznaueria barnesae and,to a lesser extent, Ephro/ithusjloralis occur in some of theblack shale layers with C -values reaching 3% TOC, whichcontain marine maceral~ (algenite, biturninite) oftype-11
kerogen and lesser amounts of terrestrial type- Ill kerogen.
Anoxia occurred only sporadically at the Cenomanian/Turonian boundary, whereas most of the Albian dark
sediments were deposited in a dysaerobic to aerobic
environment. Turbidites are most probably responsible fortransportation and preservation of calcareous nannoplankton into deeper parts of the basin in the Rio Fardes
area during the Cenomanianffuronian Boundary Event.
REFERENCES
Homeier, G. (1993): Sedimentologie, Stratigraphie und Geochemie
des Mesozoikum und Palaeogen im Medianen Subbetikum(Rio Fardes und Rio Gor, Provinz Granada, Sild-Spanien).
Thesis, Univ. TUbingen, unpublished, 126 pp.
Reicherter, K., Pletsch, T., Kuhnt, W., Manthey, J., Homeier,G., Wiedmann, J. and Thurow, J. (1994): Mid-Cretaceous
paleogeography and paleoceanography of the Betic Seaway(Betic Cordillera, Spain). Paleogeography,Paleoclimato-logy, Palaeoecology, 107, 1-33.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

MID-LATE CRETACEOUS NANNOFOSSIL BIOSTRATIGRAPHY
OF mE PAPUAN BASIN, PAPUA, NEW GUINEA
Richard Howe
Poster session

Situated on the north-eastern margin of the Australian
Plate, the Papuan Basin of Papua New Guinea has
undergone a highly complex Mesozoic and Cenozoic
tectonic and depositional history. Following early riflingin the Late Triassic and Early Jurassic, the basin developedon a passive margin in the Late Jurassic, Cretaceous andPalaeogene. Changes in relative plate motion in the late
Palaeogene, as the Australian Plate began to move north,resulted in the basin developing as a foreland basin on aconvergent margin from the late Oligocene to the presentday. Exposures of mid- and upper Cretaceous sediments of
the Basin are concentrated in the Papuan Fold Belt, where
they have been uplifted and deformed during the Neogene.
Nannofossil assemblages in the Basin have very rarely been
comprehensively described (e.g. Shafik, 1990) for the midlate Cretaceous interval, and have never been well illustrated
by published photographs.
In the western part of the Basin, around the Ok Tedi
area, mid-Cretaceous siliciclastics of the Ieru Formation
contain low to moderate diversities and abundances oflate
Aptian- Turonian nannofossils. Preservation andabundance become progressively better up-section, as the
paleobathymetry increased. These assemblages show coolwater Austral affinities, with the presence of such species
as Seribiscutum primitivum, So/lasites falklandensis andthe generally low abundance of warmer water species suchas Flabel/ites biforaminis and Rhagodiscus asper. The
Austral affinities decrease up-section into the Turonian. In
the northern part of the Basin, around the Mendi area,
upper Cretaceous calcareous siliciclastics of the Chim
formation contain moderate to well preserved Santonian
to Maastrichtian nannofossils, including some very well
pre5ervedMicula prinsii zone material from Mendi. These
assemblages show temperate to warm-water extra-tropicalaffinities, with the absence of species such as Seribiscutum
primitivum, and higher diversities than in the midCretaceous section. These assemblages confirm that the
Papuan Basin was in the Austral province of Shafik ( 1993)
during mid-Cretaceous times, and that it had a northerly
component of motion during this time which progressively
carried it into the warmer-water extra-tropical province of
Shafik (1993).

REFERENCES
Shafik, S., 1990: Late Cretaceous nannofossil
biostratigraphy and biogeography of the Australianwestern margin. Bureau of Mineral Resources, Geology
and Geophysics Report, Australian Government
Publishing Service, Canberra, 295, 164 pp.
Shafik, S., 1993: Albian and Maastrichtian nannofloral
biogeographic provinces in Western Australia. AGSO
Research Newsletter, 19, 15.

BIOSTRA TIGRAPHY IN THE OIL INDUSTRY
Martin Jakubowski
VVednesday, 15.15

Biostratigraphy is a geotechnology which has been at thefoundation of geology for many years and is an essential
discipline in hydrocarbon exploration. There are manydifferent biostratigraphic (and non-biostratigraphic)
disciplines available to the industry for the purpose ofchronostratigraphic and paleoenvironmental interpretation
and well correlation, which are reviewed. A thoroughunderstanding of the advantages and disadvantages ofthese techniques are required to ensure that abiostratigraphic study meets its objectives. The correct
combination of these techniques allows for the constructionof a sound stratigraphic framework which is essential inpredicting lateral and vertical facies changes.
The impact biostratigraphy can have on hydroqubon
exploration can only be fully realised through integration
with other geological disciplines. In recent years the conceptof sequence stratigraphy has provided the vehicle to ensurethat this integration procedure is followed to develop
geological models at reservoir, basin and regional scale.
This has led to a change in the skills profile and the function
ofbiostratigraphers in the oil industry.
Some examples of the application ofbistratigraphy inan exploration and production context are documented.

CALCAREOUS DINOFLAGELLATE CYSTS: ULTRASTRUCTURE TYPES AND
SYSTEMATIC APPLICATION
Dorothea Janofske, Helmut Keupp and Helmut Willems
Monday, 10.20 and poster session

About 20 % of living dinoflagellate species are known to
produce cysts during their life cycle but for most of the
known dinocysts the cyst-theca relationship is not yet

established. Two different taxonomic systems exist for
dinoflagellates: one based on the vegetative stage and one
based on the cyst stage. As fossil dinoflagellates are normally64=============================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

known only by their cyst stage, paleontologists have to
use the latter. Fossil dinocysts consist of acid-resistantsporopollenin:-like material (organic-walled) and/or ofcalcite(calciodinelloid). Dinoflagellates are known to have various
cyst morphotypes for one vegetative species. One clone ofcalciodinelloid dinoflagellates can produce up to fourmorphotypes simultaneously. Assemblages of fossil andrecent calcareous dinocysts show different morphotypes,
caused by variation of crystal morphology. Thin sections(2-3 J..Llll) of selected calcareous dinocysts were used for the
analysis of crystallographic patterns, and four ultrastructure
types were confirmed, on the basis of the crystallographic
orientation of the calcite crystals forming the cyst wall:
1. Radial: calcite crystals arranged with the c-axis
perpendicular to cyst surface, optic sign: negative,
symmetric extinction cross.
2. Tangential: calcite crystals arranged with the c-axis
horizontal to cyst surface, optic sign: positive, symmetric
extinction cross.
3. Oblique: calcite crystals arranged with the c-axis
inclined at various angles and directions even in one
specimen, optic sign : vague due to overlapping ofinterference colours.

Journal of Nannoplankton Research, 17, 2, 1995.
4. Pithonelloid: calcite crystals arranged in rows, theirc-axes inclined, angle and direction consistent to cyst
surface. In sections perpendicular to the longitudinal axis,
optic sign is a symmetric extinction cross.
Sections parallel to the longitudinal axis show an
asymmetric extinction cross. Interference colours dependon the specific angle of the c-axis. The different
morphotypes of one single calcareous cyst species
occurring in fossil and recent assemblages as well as inclones are characterized by variation in crystal morphology.
But, the calcite crystals forming the cyst wall always havethe same crystallographic orientation. These
crystallographic regularities are the result ofbiologicallyinduced and biologically-controlled biorninerali:zation
processes. Crystallographic orientation patterns are
regarded as a genetically fixed and primary character intaxonomy. The four different ultrastructure types based on
crystallographic orientation correspond to the subfamilies
Orthopithonelloideae (radial, Triassic - Recent),
Fuettererelloideae (tangential, Tertiary - Recent) ,Obliquipithonelloideae (oblique, Triassic- Recent) andPithonelloideae (pithonelloid, Triassic - Cretaceous) in
calciodinelloid dinoflagellates.

COMPARATIVE VARIATION OF CALCAREOUS NANNOFOSSILS (ESPECIALLY
ELLIPSAGELOSPHAERACEAE), FORAMINIFERS AND ORGANIC MATTERCONCENTRATION IN THE KIMMERIDGIAN SEQUENCE FROM LA BRIERE(NORMANDY, FRANCE)Marie-Christine Janin, Yann Samson, Moria Saint-Germes, Fran~ois Baudin and Gerard Bignot
Wednesday, 12.00
Among the highly polymorphic group of
Ellipsagelosphaeraceae, the circular forms (particularly
Cyclagelosphaera margerelii Noel, 1965) are often
considered as indicative of confined paleoenvironments.
In order to obtain more precise information about thebiological and paleoecological significance of the variabilityof Ellipsagelosphaeraceae, a detailed investigation of
calcareous nannofossil assemblages (Fig. 1, next page) has
been carried out on 35 samples from the Octeville Clay
Formation (Late Kirnmeridgian sensu gallico =ammonite
zones Mutabilis and Eudoxus) outcropping in La Briere
cliffs near Le Havre (northwestern Paris Basin: Bignot etal., 1994 ). The nannofloral variability is compared with thevariation offorarniniferal assemblages on one hand (Y.S.),
and of clay composition and carbonate and organic matter
content on the other (M.St. G and F.B.; preliminary resultsinBaudin, 1993 andSaint-Germes, 1994).
The uniform lithology (dark clay succession onlyinterrupted by a few more calcareous beds), theunchanging composition of the clay fraction, and the======================~65moderate amplitude ofthe bathyrnetrical variation indicatedby the forarniniferal assemblages suggest that no drastic
paleogeographic modification occurred in the basin during
the time interval considered. However, the calcareous
nannofloral abundance and composition seem highlyvariable, with a striking correlation between the dominanceof coccoliths ofEllipsagelosphaeraceae and the high valuesof organic matter concentration. Different hypotheses areproposed and discussed to explain this paradoxical situation.
REFERENCES
Baudin F., 1993: Etude preliminaire du contenu en matiereorganique du Kimmeridgien normand . Geologie de laFrance, 2 (1992), pp. 31-38.
Bignot G. (coord.), et al., 1994: 22eme Colloque Europeen
de Micropaleontologie, livret-guide. Rev. Micropaleontol.,
suppl. vol. 36, pp. 107-110.
Saint-Germes M ., 1994 : Sedimentologie de la matiereorganique et des argiles dans le Kimmeridgien deNormandie (region du Havre); relation avec lastratigraphie sequentielle. DEA Univ. Paris 6, 50 p.

Journal ofNannoplanlcton Research, 17, 2, 1995.

LA BRH:I!r:m

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

CALCAREOUS NANNOFOSSlL ASS!lt!HLAGJ::SCOMPOSitiON (%)
AHUNDANC~ (nb./Ueld,

50

100

m.agnlf.x790}% CaCOa

FORA!HN,

-

-

0

inner

outer .......,.........~..........._.y

shel!

shelf

% 1'0"rAL
ORGANIC CAII.BON

4.

J ....... .
Nubec.ulariids

.

z
<(

.., '
~

\
\

H

Figure 1. La Briere section, lithology, composition and abundance of nannoplanlcton assemblages, foraminifers, content of CaC03 , andtotal organic carbon.

THE CASE OF THE MISSING NANNOFOSSIL OR "NOW YOU SEE IT,NOW YOU DON'T"
David Jutson
Wednesday, 16.00

The field of nannoplankton research, both of living andfossil fonns has expanded greatly in the last twenty years.
The uses of nannofossils for paleoenvironmental
reconstructions and stratigraphy, often with very highresolution, are well-known.
Observations of nannofoSsil assemblages over time fromalmost any source reveals that nannofossils are disappearing
at significant rates from raw material and from preparedslides. In an industrial setting, this process can be observed
taking place within a few minutes of the sample from adrilling well reaching the surface. In an academic setting,within the time frame of three years, samples which havebeen stored as dry, raw reference samples have been seen

to oontain significantly impoverished nannofloras comparedto material from the same sample processed soon aftercollection.
For any nannofossil worker interested in her/his
discipline, consideration of this loss of data should be ofprimary interest as the conclusion must be that however
hard we try, we are all working with fundamentally corrupt
data sets. Unless a solution can be found to avoid the loss,
then we must accept that comparisons of qualitative andespecially quantitative analyses must be highly suspect.
This talk does not to offer a solution, but attempts to mak:enannofossil workers aware of the problem and to stimulateinterest in finding ways of solving it.

LATE PLIOCENE NANNOFOSSIL BIOEVENTS AND THEIR BIOSTRATIGRAPHIC
AND PALEOCEANOGRAPHIC MEANINGS
Koji Kameo, Tokiyuki Sato, and Toshiaki Takayama
Tuesday, 9.15

Since many authors have been studied sequential changesof nannofossil assemblages, they have establishednannofossil datums in the Quaternary sediments (fakayama

and Sato, 1987; Raffi et al., 1993; Wei, 1993, etc.).
Quaternary nannofossil datums defined by them are mainlycomposed of the first and the last occurrences of some

66==========================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

taxa, especially included into the family Prinsiaceae. Someauthors have also investigated sequential biometricalchanges of their taxa and shown gradual changes of theirsize (Matsuoka and Okada, 1989, etc.). As a result of them,it has been clarified the datums of Gephyrocapsa and
Reticulofenestra specimens ate apparently represented bysome appearances and disappearances of their larger
specimens. Sato et al. (1991) and Kameo et al. (1995)
indicated new late Pliocene biohorizons, may be composedof similar patterns of Reticulofenestra size variations
observed in the Quaternary, and possibility of their global
correlation. However, detailed size variations of them havenot been shown yet.
In this study, detailed size variations of thereticulofenestrids coccoliths in the upper Pliocene
sediments were studied in the North Atlantic DSDP cores,
Holes 606, 607 and 610A. As a result of this study, aJournal of Nannoplankton Research, 17, 2, 1995.

characteristic size fluctuation ofReticulofenestra specimens
and remarkable occurrences of other reticulofenestrids
coccoliths were found in the upper Pliocene sediments.
The size variation of Reticulofenestra specimens during
the late Pliocene is characterized by four cycles of a sizefluctuation which becomes gradually larger upward andabruptly smaller at each biohorizon. Small Gephyrocapsa
and Dictyococcites specimens were found in the limited
intervals in the upper Pliocene sediments. It is clear that the
Reticu/ofenestra size variation and the abundantoccurrence of small Gephyrocapsa are almost synchronous.
Furthermore, they can be almost traceable into the upper
Pliocene sediments not only in the North Atlantic but also
in other Oceans.
The biohorizons which were made clear by thebiometrical study of the reticulofenestrids coccoliths, thecorrelation with other areas and their paleoceanographic
meanings will be discussed.

CALCAREOUS DINOFLAGELLATES OF THE EQUATORIAL ATLANTIC OCEAN
Beate Kerntopf
Monday, 14.25 and poster session
In the equatorial Atlantic Ocean, about 25-55% of theshelled phytoplankton organisms are armoured
dinoflagellates. Data from the tropical fully oceanicplankton communities confirmed that only 8-9% of thethecate dinoflagellate species produce cysts. The cyst
assemblages are heavily dominated by calcareous forms.
Few species are found in great abundances.
Calcareous dinoflagellate resting cysts (calcareous
dinocysts) add up to 2-15% of the shelled phytoplankton.
Data from several plankton surveys (pers. comm. Janofskeand Hoell), including the present study, suggest a strong
temperature dependence of some calcareous dinocysts.
"Sphaerodinella" albatrosiana (Kamptner) and "S. "tuberosa (Kamptner) can be regarded as "warm watercysts". Their planktonic distribution is restricted to lowlatitude waters and the geographical areas defined by the
24°C SST isotherm. In waters colder than 24°C no suchcalcareous warm water cysts were recorded.
The vegetative, coccoid Thoracosphaera heimii(Lohmann) Kamptner is a more or less cosmopolitan species
which is found frequently to abundantly in the plankton
within a wide temperature and salinity range. In the waters
around the Canary Isles the relative amount ofT. heimiishells reached a maximum of 12% of the phytoplankton.
The calcareous dinocysts and T. heimii-shells are readilypreserved in the sediments. Sub-Recent multi-corer
sediment samples of the tropical East Atlantic were
investigated for calcareous dinoflagellates. The presenceor absence of the calcareous warm water cysts in thesediments can be used as an indicator for glacial SST shifts
below the "critical" 24°C-limit And, the relative abundancesof T. heimii-shells can give further information on
dinoflagellate paleoproductivity. The distribution of species
and assemblages in the sediment, compared with conditionsin the directly overlying water column, give evidence oflateral transport.
The species association in the sediments offshore NW
Africa is overwhelmingly dominated by T. heimii-shells(relative amount 80-90%); the calcareous dinocysts arepresent but only in small amounts (max. 15%). In thesediments of the Guinea Basin, however, the species
association is dominated by the warm water cysts "S. "albatrosiana (50-55%) and "S." tuberosa (12-20%). T
heimii-shells amount to 20-40%. Offshore NW Africa thespecimen densities ofT. heimii-shells are apprpximately
three times as high as in the Guinea Basin, suggesting a
productivity three times as high. And, there are only minor
shifts in the species association downcore to the LGM,
suggesting higher SST values than most foraminiferal SST
estimates.
Thus, the distribution pattern of calcareous dinocysts
can be used as a further paleoclimatic indicator, whereas
the fossil vegetative, coccoid T. heimii-shells potentiallyoffer a direct record of dinophyceae primary productivity.
Furthermore, the dinoflagellate fossil record could be reevaluated on the basis of calcareous dinocysts and T.
heimii-shell remains, at least from the Tertiary onward.

67======================~

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

CALCAREOUS DINOFLAGELLATE CYSTS OF THE LATE ALBIAN AND THEIRENVIRONMENTAL DEDUCTIONS (BOREHOLE KIRCHRODE 1/91, GERMANY)
Helmut Keupp
Poster session
The Late Albian flora of calcareous dinoflagellates recorded
from the 240 m long borehole Kirchrode I /91 (Hannover,
Lower Saxonia) contains 37 morphotaxa (cf. Keupp 1995).
There are following structural basic types represented:
I. With consequente radial orientation of wall-crystals(Orthopithonelloideae Keupp 1987): 8 Morphospecies
II. With uniquely oblique orientation of wall-crystals(Pithonelloideae ( Keupp 1987): 3 Morphospecies (cf.
Keupp and Kienel1994)
Ill. With irregularly orientated wall-crystals(Obliquipithonelloideae Keupp 1987): 26 Morphospecies
Two species are dominant: Pithonella sphaerica andObliquipithonella patriciagreeleyae type A indicative of
warmwater conditions (greenhouse climate) ofa rather distal
sedimentation area (open shelf situation: Villain 1981 ).
The assemblages react in its percentage composition tophases which are characterized by increasing water
movements particularly during transgressions. These factor
enabled also Mediterranean taxa to reach the Lower
Saxonian Basin via the Wessex Basin from the west.
Therefore, the transgressive periods of the borehole (240150 m, 90-70 m, and 25-5 m) are characterized by:-A relatively high diversity (up to 18 morphospecies/
sample) due to taphonomical mixture of the more-or-lessautochthonous neritic cysts (benthic cysts with thick,douple-layered calcareous walls) and rather pelagic cysts(normally with thin, single-layered calcareous walls)
including also few Tethyan elements (e.g.: Bicarinellumcristatum).
-Acmes, particularly of the small (23-30 J.Lm) cysts of
Obliquipithonella albiensis Keupp and Kowalski 1992.
Its morphology resembles closely the Modern vegetative
coccoid bodies of Thoracosphaera heimii.
Obliquipithonella albiensis is interpreted here to represent
rather planktonic cysts of a pelagic environment thanvegetative stages.

The interval of the borehole between 165 and 40 m
exhibits probable orbital forced cyclicity based ongeochemical, geophysical and lithological data (cf. BCCPGroup 1994). The prominent 12 m cycles correspondpossibly to eccentricity (100 000 years) . The additional
subordinate periodic cycles of8 m, 4,2 m, 3,4 m and 1, 7 m
corresponds roughly to the Milankowitch frequency band.
Some species of calcareous dinoflagellate cysts react
significantly to the 12 m-cyclicity (a more detailed view is
not possible due to every 5 m distance of investigatedsamples) by changing of sizes (smaller during carbonate
rich phases, larger during phases of pure carbonate content)suggest a cyclicity controlled by productivity.
REFERENCES
BCCP-Group, 1994: The Upper Albian of northern Germany:
Results from the Kirchrode 1/91 borehole , Boreal
Cretaceous Cycles Project (BCCP).- Zbl. Geol. Palaont. TeilI, 1993 (7 /8): 809~822; Stuttgart.
Keupp, H . (1987): Die kalkigen DinoflagellatenZ)'"te n desMittelalb bis Untercenoman von Escalles/Boulonnais(N-Frankreich).- Facies, 16: 37-88; Erlangen
Keupp, H ., 1995: Die Vertikai-Verteilung der kalkigen
Dinoflagellaten-Zysten der Bohrung Kirchrode 1/91
(Ober-Aib, NW-Deutschland).- Berl. Geowiss. Abh.,
Reihe E, 16 : 155-199; Berlin
Keupp, H . and Kienel, U., 1994: Wandstrukturen bei
Pithonelloideae (kalkige Dinoflagellaten-Zysten):
Biomineralisation und systematische Konsequenzen .- Abh.
geol. B.-A., 50 (E.FI gel-Festschrift): 197-217; Wien.
Keupp, H . and Kowalski, F.-U . (1992) : Die kalkigen
Dinoflagellaten-Zysten aus dem Alb von Folkestone/
SE-England.- Berliner geowiss. Abh., Reihe E, 3 : 211-251 ;BerlinVillain, J.-M. (1981 ): Les calcisphaerulidae: inten::tstratigraphique et paleoecologique.- Cretaceous Res.,2 : 435-438; London

DEVELOPMENT OF CALCAREOUS DINOFLAGELLATE CYSTS(CALCIODINEL~CEAE DEFLANDRE, 1947) AT THE CRETACEOUS- TERTIARY

BOUNDARY (NE GERMANY, DENMARK)
Ulrike Kienel
Poster session
Topics: calcareous nannofossils, calcareous dinoOagellate cysts, K/T boundary, Germany, Denmark

Samples originating from core Nennhausen 2/63
(Westbrandenburg, East Germany) have been investigated
for their content in calcareous nannofossils and calcareous
dinoflagellate cysts. The profile includes late early
Maastrichtian (CC24) sensu Sissingh, 1977) to lowermost
Danian (NP2 sensu Martini, 1971) sediments with anuncommonly complete record of the K!f boundary interval
for the near shore environment of this area, caused by its========================68

location in the rim syncline ofa salt diapir. The hiatus at the
K!f boundary comprises the uppermost part of CC26
(Sissingh, 1977) and the lower part of the Biantholithus
sparsus zone (van Heck and Prins, 1987).
The missing interval is, according to the correlation of
the nannofossil data, completely covered by the Danish
profiles (Stevns Klint, Nye Kl0v, Kj0lby Gaard, Bulbjerg
and Vokslev). This fact allows characterization of the6th INA Conference, Copenhagen 199~. Programme and Abstracts.

development of calcareous dinoflagellate cysts around theKff boundary.
The taxonomical study of the latter results in thedescription of numerous new genera and species. The
morphospecies Obliquipithonel/a opercu/ata,
Opercu/odinella hydria and Od. costata are recognized
as belonging to one "form-group" sensu Keupp et al. ( 1991)
with gradual transition. By including Ob/iquipithonella
opercu/ata, known by nannofossil workers as"Thoracosphaera" opercula fa, within a "form-group" ofincreasing paratabulation its long debated cyst nature canbe confirmed.

Journal of Nannoplankton Research, 17, 2, 1995.

Within the development of the calcareous dinoflagellate
cysts 4 more or less artificial stages can be recognizedfollowing the ecological stress at the Kff boundary. This
stages allow to infer a similar development within thecalcareous dinoflagellate cyst assemblages to that known
from the calcareous nannofossils. It is characterized (besides
the persisting forms without any reactions) by the"surviving" of "stress" -forms, showing bloom likeabundances (Lentodinel/a danica and Ob/iquipithonella
operculata), from which later the new morphospecies seemto have derived.

A 300 KYRS CALCAREOUS PLANKTON RECORD OF THE EQUATORIAL
SOUTH ATLANTIC: RECONSTRUCTIONS OF SURFACE WATER PRODUCTIVITY
AND BOTTOM WATER DISSOLUTION CYCLES
H. Kinke/, N Dittert, K.H. Baumann
Poster session

Pelagic cartxmate fluxes from surface waters to the sedimentand carbonate dissolution in the water column and at the
sediment water interface Play an important role in the carbon
cycle of the oceans and the atmosphere. In the Late
Quaternary fundamental changes occured in the carbon
cycle, which are documented in alternating sedimentationof calcium carbonate in the deep sea; they are explained as
cycles of productivity, dilution, dissolution, and diagenesis.
While productivity responds directly to changing climates
via the wind driven equatorial upwelling system in theprecessional band (23 kyr) the preservation/dissolution ismore indirectly controlled by the production rate ofNorth
Atlantic Deep Water (NADW) in the eccentricity band
(lOOkyr).
The synoptic and quantitative record of planktonic
foraminifera and coccolith assemblages in glacial/interglacial sediment sequences of the Late Quaternary

South Atlantic follows an synecological analysis andinterpretation.
The investigation of carbonate tests according to thepartial respectively the complete di~solution refers to thesurrounding water masses. Methods are the conventional
fragment index, dissolution indices (REM), and thecomparison between heavy dissoluted forarninifera and thepoor preservated coccoliths.
·
The changes in the surface water masses are well
documented in the species composition of planktonic
forarninifera and coccolith assemblages. The changing
bottom water distribution is documented by changing
carbonate contents and accumulation rates, andconventional fragmentation and dissolution indices ofplanktonic forarninifera. Dissolution indices for coccoliths,
however, are difficult to establish, but, the general trend in
the preservation of the whole coccolith assemblage can becorrelated to the dissolution indices of planktonic
foraminifera.

THE MIOCENE BLUE CLAY FORMATION OF mE MALTESE ISLANDS:SEQUENCE- STRATIGRAPHIC AND PALEOCEANOGRAPIDC IMPLICATIONSBASED ON CALCAREOUS NANNOFOSSIL STRA TIGRAPHY AND CALCAREOUS
DINOFLAGELLATE CYSTS
U. Kiene/, U. Rehfe/d, S. Bel/as and R. Kohring
Poster session
Topics: Calcareous nannofossils, calcareous dinona.:ellate cysts, paleooceano.:raphy, sequence strati1raphy, Miocene,Blue Clay, Maltese Islands

Samples from the Middle to Upper Miocene strata of the
Maltese Islands have been investigated for their content incalcareous nannofossils and calcareous dinoflagellate cysts.
The sediments under consideration have been deposited
on a submerged carbonate platform; they comprise theupper part of the Upper Globigerina Limestone, the Blue
Clay and the 1owermost Greensand Formation. They cover
the time interval between the NN5 zone (Langhian) to=========================69

NNllb subzone (Messinian), with two conspicuous
biostratigraphical hialllses in between.
The Catinaster coa/itus zone (NN8 sensu Martini andWorsley, 1970) has been proved for the first time on the
Maltese Islands. The occurrence of undifferentiatedCatinaster-like individuals interpreted as early forms of
Catinaster calyculus and small Catinaster sp., areconsidered as indicators of the upper part of the C. coali tus

Journal of Nannoplankton Research, 17, 2, 199S.

6th INA Conference, Copenhagen 199S, Programme and Abstracts.

zone appearing below the FO of Discoaster hamatus NN9zone). The nannofossil assemblage from the Greensand
Formation exhibits strong reworking reflected by theoccurrence of C. jloridanus and C. nitescens. The presenceof Discoaster icarus. D. pansus. D. surculus as well as A.
primus provides strong evidence that the base of theGreensand belongs into the NN11b subzone.
Few calcareous dinoflagellate cysts have beenrecorded. The dominating species, Orthopithonel/agranifera exhibits a great variability in crystal size andovergrowth pattern. Additionally, the stratigraphic rangeof the obliquipithonelloid species Bicarinellum
tricarinelloides (up to now known from Pleistocene to
Recent), can be traced back to the Serravallian.
In general, the recorded calcareous dinoflagellate cysts
are mainly dominated by orthopithonelloid andfuettererelloid species, indicating open marine, pelagic
conditions.
The first hiatus, within the upper part of the Blue Clay
Formation, comprises about 100 ky (top NN7 to upper part

NN8- uppermost Serravallian). It corresponds to the second
order Sequence Boundary at the transition from supercycles
TB2 to TB3 according to the global sea level chart ofHaq
et al. (1988). It comprises the time of the NH4 deep seahiatus related to increased ice build-up in the Antarctic
region. After a very short time of reestablishedsedimentation (about 100 ky) a second hiatus follows
immediately on top ofthe NN8 zone (Serravallian!fortonianboundary). It lasted as long as 3.7-3.9 my to the NNllb
subzone; thus the whole time of the Tortonian and probably
the lower part of the Messinian elapsed between thedeposition of the Blue Clay and Greensand Formation. This
time span comprises the narrowly spaced deep sea-hiatuses
NH4 to NH6. A cooling of surface waters on the Maltese
Platform is partially substantiated by the calcareous
nannofossil assemblages. An earlier cooling event may besketched by the gradual transition from the Globigerina
Limestone carbonate deposits to the siliciclastic sedimentsof the Blue Clay Formation.

CALCAREOUS NANNOPLANKTON RESPONSE TO TERMINATION 11 AND
HEINRICH EVENT (140-llOKABP) IN THE NE ATLANTIC
Anna Lotoskaya and Patrizia Ziveri
Poster session

First results on carbonate fluxes in the NE Atlantic during
the last interglacial have been obtained from the pelagic
piston-core T90-9P (45°17.5' N; 25°41.3' W) raised from the
Mid-Atlantic Ridge. The last interglacial (Termination II,
oxygen isotope stage Se) covers the time interval between
140 and 110 ka BP, and is considered to be the strongest
warming during the Quaternary. Quantitative analyses ofcalcareous nannofossils have been carried out in order toknow coccolith-paleo-fluxe during the previous
deglaciation. Each sample was first wet sieved over 32 lliil
mesh using 2liters of tap water; then the finer fraction has
been processed with solutions ofNa4Pp7 and ~02 to get
equal distribution of the material on the filter. Afterwards
0.15 ml ofobtained solution has been filtered with a Millipore
filter(47 mm diameter, 0.45J.Lmporesize). Proportions of
the filter have been used for quantitative polarised
microscope and SEM study. Fraction >32 J.Lm in size has
been checked semiquantitatively with a binocular
microscope.
A count of 350-400 specimens of coccoliths wereidentified and quantified (plus about 100 specimens of rare
species) in the fine fraction using a polarized lightmicroscope by analyzing a defined area of each filter.
Terrigenous material, detrital carbonate am foramfragments
were taken into account. The counted particles have been
extrapolated for the entire sample in order to calculate thenumber of coccoliths per gram of fine fraction, relative
abundances of different species in the coccolith assemblage
and the role of non-coccolith material in the sediments.
Total and fine fraction carbonate content, and oxygenisotope stratigraphy are also investigated.
The results show that calcareous nannoplankton appear
to be the main carbonate producers in the NE Atlantic deep==========================70

sea. Fluctuations in carbonate content (total and fine
fraction), percentage of mineral particles (mostly quartz)
and detrital carbonate in both fractions, coccolith flux anddistribution of different nannoplankton species show thepresence of a Heinrich layer composed of debris, probably
released during the melting of massive influxes of icebergs
into the North Atlantic. This event coincides with the periodof the strongest temperature changes in the sedimentrecord. Distribution patterns of Florisphaera profunda
increasing in abundance during the Heinrich event, support
the idea of this species being an indicator of sea-water
turbidity, as it was recently shown for the Quaternary of
the Pacific (Ahagon et al., 1993).1t is known thatF profunda
lives exclusively in the lower euphotic zone (Okada andHonjo, 1973), so reductions in light caused by iceberg
discharges didn't influence its abundance, whereas the
production of all other species was diminished.
The middle part of the studied interval corresponding
to the Termination itself, is characterised by appearance ofthe tropical water species Umbellosphaera tenuis andU.irregularis (Mclntyre and Be, 1967), and significant
decrease in subarctic species Cocco/ithus pelagicus(Mclntyre and Be, 1967) and Helicosphaera carteri which
had been described as a species preferring cold waters(Bartolini, 1970). Calcidiscus leptoporus and Gephyrocapsa oceanica distribution don't show any fluctuations
directly related to studied parameters. The "small
placoliths", iocluding small-medium sile Gephyrocapsa andsubordinated Emi/iania huxleyi, make up to 94% of thecoccolith assemblage. The taxonomic identification of thisgroup will be studied separately with the SEM.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

REFERENCES

Estimated absolute numbers of coccoliths per gram ofsediment vary from 7xl 0 8 in the Heinri.ch layer to 15x lO 9
liths/g sediment in the coccolith ooze. These results don't
show good correlation with carbonate content variations
due to different methods of sample preparation in the earlystages. But it's possible to state that decreases in coccolithand planktonic foraminifera remains are not high, and arecaused mostly by dilution, rapid debris accumulation, andpartly by reduction in plankton productivity (as a result oflight obstruction due to spread of icebergs).

Ahagon, N., Y.Tanaka, and H. Ujiie , 1993 . Florisphaera
profunda, a possible nannoplankton indicator of late
Quaternary changes in sea-water turbidity at the northwestern margin of the Pacific. Mar. Micropal., 22: 255-273.
Bartolini, C., 1970. Coccoliths from sediments of the western
Mediterranean. Micropal., 16(2): 129-154.
Mclntyre, A. and A.W.H. Be, 1967. Modern Coccolithophoridae of the Atlantic Ocean-!. Placoliths and Cyrtoliths.
Deep-Sea Res., 14: 561-597.
Okada, H., and S. Honjo, 1973. The distribution of oceanic coccolithophorids in the Pacific. Deep-Sea Res., 20: 355-374.

CALCAREOUS NANNOPLANKTON BIOSTRATIGRAPHIC ANALYSIS AS A TOOLFOR THE STUDY OF DISCONTINUITY SURFACES IN mE CRETACEOUS OF
THE TRENTO PLATEAU (SOUTHERN ALPINE, ITALY)Francesca Lazar
Wednesday, 11.3 5characterized by: 1) a flat surface on which lays a thinchaotic layer (debris flow), with rounded lithoclasts
belonging to the underlying Biancone; 2) deep burrowingof the underlying limestones; the burrows infill is a red
rnicritic limestone containing planktonic forarninifera; 3) a
glauconitic mineralization wrapping the clasts and the chert
nodules in the chaotic level, sometimes (Lenzi.ma) covering
the entire surface.
The detailed biostratigraphic analysis; performed withcalcareous nannofossils and planktonic foraminifera,
allowed to infer the age of the topmost Biancone strata, of
the burrow infills and of the overlying Scaglia Variegata.
These are: Early Aptian for the top of the Biancone, Late
Aptian for the burrow infills and Late Albian for theoverlying Scaglia Variegata. This clearly shows thatdifferent sedimentological evidences (hard ground, debris
flow and burrowing at Monte Altissimo, debris flow at
Molveno and hard ground at Lenzim), in fact represent thesame time gap in the sedimentary record, thus confirmingthat major discontinuity can have the same genetic
significance.

Several discontinuity surfaces recognized in the Cretaceoussequence of the Southern Alps are in study at the
Dipartimento di Scienze della Terra in Torino.
During the Cretaceous the Trento Plateau experienced
a mainly pelagic carbonatic sedimentation, apparently very
continuous and without major gaps. The Cretaceous
sediments are represented by Biancone, Scaglia Variegata
and Scaglia Rossa Formations.
In the pelagic environment represented by theformations listed above, the tecton-ic and/or
paleoceanographic events caused several discontinuity
surfaces (at the Cretaceous!fertiary boundary, during theCampanian, during the Aptian-Albian). This preliminary
study deals with the discontinuity located in the AptianAlbian time interval, marked by sharp lithologic change
and underlined by a hard ground surface, and/or byburrowings or sometimes without sedimentologicalevidence.
In the Monte Altissimo and Molveno areas this
discontinuity surface occurs at the boundary between
Biancone and Scaglia Variegata Formations p. From thelithologic point of view, this surface is, in general,

PLEISTOCENE CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF SITE 577
LEG 86, NORTHWESTERN PACIFIC OCEAN
Patrizia Maiorano, Maria Marino and Simonetta Monechi
Poster session
A detailed biostratigraphic study has been performed on
Pleistocene sediments of Site 577 of the Shatsky Rise.
Previous studies (Monechi, 1985; Monechi et al., 1985)
evidenced the good recovery by hydraulic-piston coresand the fairly complete sedimentary sequence in both holes(Hole 577 and Hole 577A).
Semiquantitative analyses on abundant and wellpreserved calcareous nannofossil assemblages has allowed
recognize a succession of events that improve the resolution

Gephyrocapsa caribbeanica, LO Ca/cidiscus macintyrei,
FO G. oceanica s.l. (sensu Rio, 1982), FO large
Gephyrocapsa (sensu Rio, 1982), LO large Gephyrocapsa,
bottom temporary disappearance G. oceanica s.l., FO
Reticu/ofenestra asanoi, FOG. para/le/a (Gephyrocapsa
sp.3, sensu Rio, 1982), re-occurrence G. oceanica s.l.,bottom temporary disappearance G. para/le/a, FO
He/icosphaera inversa, re-occurrence G. para/le/a, LO H.
. inversa, FOE. huxleyi.

of the Pleistocene interval (between the LO Discoaster

Many of the recognized events have a world-wide

brouweri and FO Emi/iania huxleyi): LO D. brouweri, FO

distribution and have been used to define the Zones of71

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Okada and Bukry (1980), Rio et al. (1990) for theMediterranean and Sato et al. ( 1991) for the Arabian Sea.
Few supplementary events such as the G. caribbeanica
and Dictyococccites productus acme in the upper part of
MNN 19f have been observed.
The succession of the nannofossil events and theircorrelation with magnetostratigraphy (Bleil, 1985) is mostly
in agreement with the literature data. A major problem
regards the LO of H sellii; in both the holes, this event isrecorded in the latest Pliocene shortly below the Olduvai
subchron, confirming the already known diachroneity of
the LO of the species, although the event has been generally
recorded above the Olduvai subchrone. The FO ofR. asanoi
occurs below the Jaramillo subchrone, according to Satoet al. ( 1991 ), Matzuoka and Okada ( 1989); the LO of R.
asanoi occurs at the top of Jaramillo subchrone and this is
not in agreement with the calibration of Matzuoka andOkada (1989). The FO of G. para/le/a occurs at the top of
Jaramillo, aceording to Takayama and Sato ( 1987), Sato etal. (1991) and Castradori (1993).
Quantitative nannofossil biostratigraphic investigations are in progress in order to define more precisely the
succession of all the recognized events and to give further
details about the beginning and the end of acme of G.
caribbeanica and Dictyococcites productus.

Castradori D. ( 1993 )-Calcareous nannofossil biostratigraphy and biochronology in eastern Mediterranean deep-sea cores. Riv. It. Paleont. Strat., 99, 107126.
Matsuoka H. and Okada H. (1989)- Quantitative analysisof Quaternary nannoplankton in the Subtropical
Nothwestern Pacific Ocean. - Mar. Micropaleontology,
14: 97-118.
Monechi S. (1985) - Campanian to Pleistocene calcareous
nannofossil stratigraphy from the Northwest Pacific
Ocean, Deep Sea Drilling Project Leg 86. In Heath G.R.,
Burlde L.H. et al., DSDP !nit. Repts., 86: 301-336.
Monechi S., Bleil U. and Backman J. (1985) Magnetobiochronology of late Cretaceous-Paleogene
and late Cenozoic pelagic sedimentary sequences fromthe Northwest Pacific (Deep Sea Drilling Project, Leg
86, Site 577). In Heath G.R., Burkle L.H. et al., DSDP
/nit. Repts., 86: 787-797.
Okada H. and Bukry D. (1980) - Supplementary modificationand introduction code numbers to the low-latitude
coccolith biostratigraphic zonation (Bukry, 1973; 1975).
Mar. Micropaleontology, 5: 335-353.
Rio D., Raffi I. and Villa G. (1990) - Pliocene-Pieistocene
calcareous nannofossil distribution patterns in theWestern Mediterranean. In: Kastens K.A., Mascle J. etal.,Proc. ODP, Sci. Results, 107: 513-533.
Sato T., Kameo K. and Takayama T. (1991)- Coccolith
biostratigraphy of the Arabian Sea. In Prell W. L.,
Niitsuma N. et al., Proc. ODP, Sci. Results, 117: 37-54.
Takayama T. and Sato T. (1987) - Coccolith biostratigraphyof the North Atlantic Ocean, Deep Sea Drilling Project
Leg 94. In: Ruddiman W.F., .Kidd R.B., Thomas E. et al.,DSDP !nit. Repts., 94: 651-702.

REFERENCES
Bleil U. (1985) - The magnetostratigraphy of northwest
Pacific sediments, Deep Sea Drilling Project Leg 86. In
Heath G.R., Burkle L.H. et al., DSDP !nit. Repts., 86:441458.

CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF EARLY- MIDDLE
PLEISTOCENE TERRIGENOUS SEDIMENTS (SOUTHERN ITALY)Maria Marino
Poster session

An early-middle Pleistocene succession of terrigenous
sediments, 400 metres thick, outcrops west ofMontalbano
Ionico (Southern Apennine Foredeep, Italy). The
reconstructed section is mainly made up of marine silty
clays interbedded by nine thin volcaniclastic layers showing
undersatured alkaline chemistry (Ciaranfi et al., 1994;
Ciaranfi et al., in prep.). Preliminary paleomagnetic
investigations pointed out the bottom and the top of
Jaramillo subchrone and the Matuyama-Brunhes boundary(Channell, pers. corn., in Ciaranfi et al., 1994).
The calcareous nannofossils quantitative
biostratigraphy led to the recognition the large
Gephyrocapsa, small Gephyrocapsa and Pseudoemiliania/acunosa Zone, according to the scheme of Rio et al. (1990).
Particulary, despite of"diluted" nannofossil assemblages
and the rarity of meaningful markers, several events wererecognized: last occurrence oflarge Gephyrocapsa, botton
acme of Reticulofenestra asanoi, top acme of R. asanoi,
end acme of small Gephyrocapsa, first occurrence ofGephyrocapsa para/le/a (Gephyrocapsa sp.3, sensu Rio,
1982), temporary disappearance of G. para/le/a and re-entry of this species. The biostratigaphic data are inagreement with preliminary paleomagnetic results,
according to biochronology by Castradori (1992; 1993):
the top of Jaramillo occurs just below the FO of G. para/lela(top of small Gephyrocapsa Zone) and the MatuyamaBrunhes boundary occurs close to the re-entry of G.
paral/ela.
Moreover, biostratigraphic work in progress seems toshow peculiar abundance patterns of some "minor" species(Syracosphaera spp., Rhabdosphaera spp.) with respect
to sapropelitic (?) interval characterizing the upper part ofMontalbano lonico succession.
REFERENCES
Castradori D. - 1992 -I nannofossili calcarei come strumento perlo studio biostratigrafico e paleoceanografico del Quaternario
nel Mediterraneo orientate. Tesi di Dottorato, Univ. degli Studi
di Milano, 216 pp.
Castradori D. - 1993 - Calcareous nannofossil biostratigraphy
and biochronology in eastern Mediterranean deep-sea cores.
Riv. It. Paleont. Strat., 99, 107-126.

72==========================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Ciaranfi N., D' Alessandro A., Marino M. and Sabato L. 1994 - La successione argillosa infra e mediopleistocenicadella parte sudoccidentale della Fossa bradanica: laSezione di Montalbano Jonico in Basilicata. In "Guida alle
escursioni" de/77_ Congresso Nazionale del/aS. G.!.; Quad.
Bib/. Prov. Matera, 15, 117-156, Venosa.
Rio D., - 1982 - The fossil distribution of Coccolithophore

Journal of Nannoplankton Research, 17, 2, 1995.

Genus Gephyrocapsa Kamptner and related PlioPieistocene chronostratigraphic problems. lnit. Repts.
DSDP, 68, 325-343.
Rio D., Raffi I. and Villa G. - 1990 - Pliocene-Pleistocene
calcareous nannofossil distribution patterns in thewestern Mediterranean. In Kastens K., Mascle J. et al.,1990, Proc. 0. D. P., Scient. Results, 107,513-533.

CALCAREOUS NANNOFOSSIL BIOSTRATIGRAPHY OF mE LATECRETACEOUS- EARLY TERTIARY OF WADI FEIRAN ANDGEBEL QABELIA T, SOUrn WESTERN SINAI, EGYPT
Akhma/ M Marzouk and Mohamed K. Abou-E/-Enein
Tuesday, 12.00
The biostratigraphic study of the Late Cretaceous - Early
Tertiary rocks of Wadi Feiran and Gebel Qabeliat, Southwestern Sinai has revealed the presence of several
calcareous nannofossils biozones. A Cretaceousffertiary
faunal break is present in the two studied sections, but themagnitude of the hiatus is greater to the south at Gebel

Qabeliat. This boundary here occurs somewhere at the topof the Sudr Chalk at W. Feiran section and in the lowennost
part of the Esna Shale at G. Qabeliat section. No faunal
break was observed within the Esna Shale of the Paleocene/
Eocene boundary~ the studied sections.

CALCAREOUS NANNOFOSSILS BIOSTRATIGRAPHY OF THE FUENTELSAZ(SPAIN) AND FIUMINATA (ITALY) SECTIONS:LATE TOARCIAN- EARLY AALENIAN
Emanue/a Mattioli and Nico/a Perilli
Poster session
Topics: late Toardan-early Aalenlan, Spain, Italy, Blostratlgraphy

Semiquantitative and quantitative analyses have been
carried out on late Toarcian- early Aalenian fairly regularalternation of limestone and marlstone deposits of theCastilian Branch (Iberian Range) and of the UmbriaMarche basin (Central Apennine ). The Fuentelsaz section
is an exceptionally thick and uniform succession which has
been recently proposed as a possible stratotype for thebase of the Aalenian stage, since it is characterized by avery rich, well-preserved and complete succession ofammonite assemblages. In this section, detailed
biostratigraphical (brachiopods, foraminifers andostracods) and sedimentological studies have been also
performed (1 and references therein). Likewise, theFiuminata section is a continuous thick and superbly
exposed late Toarcian-early Aalenian succession
characterized by well-preserved microfossil assemblages.
Here also, detailed biostratigraphical (foraminifers),
sedimentological and rnagnetostratigraphical studies havebeen carried out (2, 3 and references therein). At present,in the Tethyan areas several data on the Domerian-Toarcian
and on the Aalenian-Bajocian time intervals are available
in the literature and the nanno-biostratigraphy resolution
is quite high. On the other hand, published works on the
Toarcian-Aalenian boundary are few and further
investigations are required to detect a good and reliablesequence of events. Aim of this work is to investigate thelate Toarcian-early Aalenian interval in order to recognize
the sequence of major and minor calcareous nannofossil=========================73

events, and to compare the composition of the assemblagesof the two sections. The Fuentelsaz section is located 170
km NE of Madrid (NE of the Guadalajara province). It is 32
m thick and encompasses the Turmiel (4) and the Chelva
Fms (5). The Turmiel Fm. consists of a rhythmic alternancebetween marlstones and limestones, which are represented
by mudstones and, subordinately, bioclastic wackestones,
sedirnented on a platform or external ramp environment (6,7). The lower part ofthe Chelva Fm. is made up of limestones,
mainly represented by wackestones and rare packstones,
with intercalations of marlstones, and it is sedimented on
an external platform with very little influx of fine clastic
material (6). Fine shelled bivalves, fragments ofechinoderms
and gastropods have been found in some levels, whereas
bioturbation is frequent.
The Fiuminata section outcrops 190 km NE of Roma
(Eastern Umbria) and it consists of 30 m thick of the Calcari
e Mame a Posidonia Unit (2 and references therein). At
Fiuminata, a regular alternation of light brown rnarlylimestones and marlstones crops out and represents a good
example of a dm-scale pelagic rhythmic sedimentation. The
marly limestones are locally bioturbated and nodular
limestones are present. Posidonia shells are very common,
both in the marly and in the carbonate lithotypes (2, 3).
The succession, referable to an active subsiding furrow (8),is characterized by a considerable amount of clay, if
compared to other Umbria-Marche sections. This study isJournal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

focused on more than 200 samples, closely collected fromdifferent lithotypes. A total of 250-350 specimens werecounted in each smear slide, under a polarizing lightmicroscope at about 1OOOX magnification. Six classes of
total and specific abundance and four classes ofpreservation have been distinguished. Preliminary data fromthe studied sections reveal an overall similar assemblage
composition. In the late Toarcian, radiating placoliths,
Biscutum spp. and Discorhabdus spp. are very common;in particular, the genus Biscutum shows a great diversity.
Calycu/aceae are common and mainly represented by
Carinolithus superbus; however, Calyculus spp. shows adecreasing trend, which is a prelude to the disappearanceof the smaller form. Watznaueriaceae are common, welldiversified and mainly represented by species of the genus
Lotharingius; Watznaueria sp. 1 is the first species of thegenus to appear, and it is already present from the base of
the sections. The Toarcian-Aalenian transition ischaracterized by the first occurrence of Watznaueria
contracta and Hexalithus magharensis, and by a lightdecrease of the genera Lotharingius and Carinolithus.
Some Early Liassic specimens are still present: protoliths(Mitrolithus spp.) whith sporadic occurrences, whereas
loxoliths (Crepidolithus spp., Tubirhabdus patulus) witha background noise. Schizosphaerella spp. is constantly
present in great abundance.

(I) Goy A., Ureta S., Arias C., Canales M. L., Garcia Joral F.,
Herrero C ., Martinez G. and Perilli N., 1994 - The
Fuentelsaz section (Iberian range, Spain), a possible
Stratotype for the base of the Aalenian Stage. Proc. 3rd
Intern . Meeting on Aalenian and Bajocian Strat. ,Miscellanea Serv. Geol. It., 5, pp. 1- 31.
(2) Morettini E. and Monaco P., 1994- Marl-limestonerhythmites and event beds in the Toarcian- Aalenian
Calcari e Marne a Posidonia Unit of Fiuminata (Pioraco,
Umbria-Marche Apennines). Eel. Geol. Helv., in press.
(3) Mattioli E., 1994 - Calcareous nannofossils of the
Toarcian-Aalenian of the Fiuminata section (Central
Apennines, Italy). Palaeopelagos, 4, pp. 175-187.
(4) Goy A., Gomez J.J. and Yebenes A., 1976 -El Jurasico dela Rama Castellana de la Cordillera Iberica (mitad Norte). ·1
Unidades Litoestratigraficas. Estudios geol., 32 , pp.
291-423.
(5) Gomez J .J . and Goy A., 1979 - Las unidades
litoestratigraficas del Jurasico medio y superior, en
facies carbonatadas del Sector Levantino de laCordillera Iberica. Est. Geol., 35, pp. 569-598, Madrid.
(6) Gomez (in Gabaldon et alii 1991)- Mapa geologico deEspana . Esc. 1.200.000 (1 edicion). Explicacion de la
Hoja n.. (Daroca). IGME.
(7) Comas-Rengifo M.J., Goy A. and Yebenes A. 1985 - Le
Lias dans La Rambla del Salto (Sierra Palomera, Teruel).
Strata, 2(2), pp. 123-142(8) Mattioli E., in progress - Quantitative analysis of
palcareous nannofossils in the limestone-marl coupletsof the Toarcian-Aalenian Fiuminata sequence (UmbriaMarche Apennine, Central Italy).

REFERENCESCALCAREOUS NANNOFOSSIL ASSEMBLAGES IN THE CENOMANIAN AND
TURONIAN DEPOSITS IN LITHUANIA
Romualda Mertiniene
The deposits of the Cenomanian and Turonian are widely
spread in Lithuania. They are represented by the terrigene
sandy sediments in the western part and by the
carbonaceous -the marI and the chalk - in the east side of
the basin. The intercalations of the sand are frequent intheir lower part.
The nannoplankton from the deposits was investigated.
Rare and badly preserved nannofossils Watznaueria sp.,
Prediscosphaera sp., Manivitel/a sp. were found in green
carbonaceous sands (Lower-Middle Cenomanian). The
growth of the nannoplankton is observed when the quantityof the carbonate increases in the deposits . The
nannoplankton is abundant and well preserved in the green
porous limestone (Upper Cenomanian): Microrhabdulus

decoratus, Gartnerago oliquum, Watznaueria barnesae,
Eiffellithus turriseiffeli, Prediscosphaera cretacea,
Broinsonia enormis, Zygodiscus bussoni, Z.
diplogrammus, Cretorhabdus conicus etc. (there are 22
species in all);
The taxonomical composition of the assemblage does
not change in the argillaceous chalk, which superpose overthe limestone. There only the increase of the quantity ofnannofossils is observed. The chalk of the Upper

74

Cenomanian pass to the Lower Turonian light grey chalkwithout any visible change. The assemblage of thenannofossils is rich. The bed is marked by the first
appearance of Quadrum pyramidum. There is a lot of

Watznaueria barnesae , Prediscosphaera cretacea,
Zygodiscus diplogrammes, z. variatus, Gartnerago
obliquum, Microrhabdulus decoratus, Biscutum sp.,
Lithraphidites carnio/ensis, Cretorhabdtfs conicus,
Eiffellithus turriseiffeli etc. (there are 26 species in all).
Kamptnerius magni.ficus appears in the middle of theLower Turonian. The nannoplankton assemblage is similar
to that from the lower part of the grey chalk (there are 34
species in all).
The top of the Upper Turonian is indicated by the first
appearance of Lucianorhabdus ma/eformis. The
assemblage is composed by Kamptnerius magnificus,

Cretarhabdus surrirelus, Lithastrinus flora/is, Eif.fol/ithus
turriseif.foli, Quadrum pyramidum, Watznaueria barnesae
etc. (there are 35 species in all).
The analysis of the assemblages of the nannoplanktonshows that there was a close connection between the floraof the Late Cenomanian and the Turonian.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995.

NANNOPLANKTON ZONES IN THE VOLCANIC TUFFS OF THE
TRANSYLVANIAN BASIN (MIOCENE)
JVico/ae A1eszaros
Tuesday, 9.40
The Transylvanian Basin constitutes a Tertiary intramountain basin lying within the internal zone of the
Carpathian Mountains. The complex basin history
commenced with the emplacement of internal nappes of
the Carpathians during the Albian continental collision.
The nappes contain allochtonous metamorphic basementand Late Jurassic calc-alkaline volcanics overlain by lateJurassic-Early Cretaceous platform carbonates and deeper
marine clastics. The overlying sediment, in an overall"piggy-back" setting reflects the complex interaction of
the Tethyan sea level variations with the active
compressional regime of the evolving Carpathian Mountainchain.
Four major tectonic phases subdivide the Transylvanianbasin fill into distinct tectonic stratigraphic units: Late
Cretaceous-Paleocene (Laramian), Eocene (Laramian
reactivation), Early Miocene (Old Styrian) and MidMiocene (New Styrian). Following the Albian continental
collision, post-tectonic Senonian clastics were depositedin a subsiding north-south trending basin, subsequently
deformed and up-crusted during the Laramian phase. The
overlying Early Eocene red bed sequence was also deposit
in a subsiding north-south trending basin, and locallyinverted in the Lutetian. This inversion created an emerged
north-south ridge controlling the paleogeography andlateral extent of two subsequent Late Eocene marinetransgressive events. In the Early Oligocene a regionaldrowning of the basin occurred and Rupelian black organic
rich shales were deposit as a draping unit. In the overlying
sequence, clastic input from the north-west was deposited

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- ~
~

<:

l&.J

~

Cl
'oq'
Q:)

1

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l&.J

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menf ~zones

STRAT/6RAPHICAL UNITES

A6£

<:

as shallow marine sandstones in marginal parts of the basin
whereas outer selfmarls was deposit in central parts of thebasin.
The major reorganization of the Transylvanian Basinoccurred in the Mid-Miocene (New Styrian phase), when
the basin acquired its present configuration. This
reorganization is linked with the emplacement of the east
Carpathian nappes. Transgressive clastics, marls and tuffs
were deposited, followed by deep marine salt layers. The
basin fill history ends with the deposition of a rapidly
subsiding Mid-Late Miocene brackish clastic sequence withmany tuffs intercalations (Fig. 1).
The nannoplankton assemblages recorded in the marlsof the Dej Tuffs are assigned to the zone NN5 (i.e. the zone
with Spheno/othus heteromorphus). The Ocna DejuluiBeds, which comprises the evaporites with gypsum andsalt, belongs to the zone NN5 too.
The next level of volcanic tuffs is the Borsa-Apahida
Tuffs, which contain assemblages of nannoplankton
assigned to zone NN6. This level is followed by the H d reni
Tuffs which are correlated to the NN7 zone, and by theGhiri~ Tuffs, which correspond to the NN8 zone. This levelis followed by the S rm sel, the Urea Tuffs, and the Sincai
Tuffs which all are correlated to NN9 zone. It should be
noted, that a precise dating of the deposits overlying thesalt has been possible by the study of nannoplankton within
the volcanic tuffs. The nannoplankton assemblages
between the tufflayers contain huge amount of reworked
Late Cretaceous and Paleogene forms, but only few
Miocene specimens.

"-'~

~""

~

"{

~

~

Dkada andBukry

!j!NCAI TUFFS (Band Ri'ciu J + + +NN9

CN 7,a,b

++ +
+++

NN9
NN9

CN 7,a,b
CN 7.a,b

~URCA

TUFFS
~~SARHA~L TUffS;JS (Colina, Zau J

fi!.6HIRI!j TUFFS fRotbav,Gn"nari) + + +HAD.4RENI TUFFS++++++(Bwfa, Cara, Ocna Murt!f)/CLOD BEDS
+ ++1 ~~~fi$Ai£1fA!//(J4 TUFFSOCNA DEJULUI BEDS
(Salt, Gypsum J+++( Ciceu·Giurgefti Formation,Podeni

limestone)

.c:
1:1

c...
'l)

~fi

DEJ TUFFS~..."' ~

NN8
NN7

CN 6
CN Sb

71,8
Deepermarine

NN6

CN Sa

NNS

CN 3,4NNS

CN 3,413,6Lagonaljevop:r;e
Oufer
shelf
[16_6

75======================~

6th INA Conference, Copenhagen 199.5, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 199.5.

NANNOPLANKTON ZONES IN THE VOLCANIC TUFFS OF THE
TRANSYLVANIAN BASIN (MIOCENE)
Nicolae Mesztiros

Tuesday, 9.40
The Transylvanian Basin constitutes a Tertiary intramountain basin lying within the internal zone of the
Carpathian Mountains. The complex basin history
commenced with the emplacement of internal nappes of
the Carpathians during the Albian continental collision.
The nappes contain allochtonous metamorphic basementand Late Jurassic calc-alkaline volcanics overlain by lateJurassic-Early Cretaceous platform carbonates and deeper
marine clastics. The overlying sediment, in an overall"piggy-back" setting reflects the complex interaction of
the Tethyan sea level variations with the active
compressional regime of the evolving Carpathian Mountainchain.

Four major tectonic phases subdivide the Transylvanianbasin fill into distinct tectonic stratigraphic units: Late
Cretaceous-Paleocene (Laramian), Eocene (Laramian
reactivation), Early Miocene (Old Styrian) and MidMiocene (New Styrian). Following the Albian continental
collision, post-tectonic Senonian clastics were depositedin a subsiding north-south trending basin, subsequently
deformed and up-crusted during the Lararnian phase. The
overlying Early Eocene red bed sequence was also deposit
in a subsiding north-south trending basin, and locallyinverted in the Lutetian. This inversion created an emerged
north-south ridge controlling the paleogeography andlateral extent of two subsequent Late Eocene marinetransgressive events. In the Early Oligocene a regionaldrowning of the basin occurred and Rupelian black organic
rich shales were deposit as a draping unit. In the overlying
sequence, clastic input from the north-west was deposited~C::IIi<: lc£i·811i"'-'-.._.,.
~~·\.Jl.::"'

Q::

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~

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~

~

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et)

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IU~

~'<:(

~
f5

~

Okada andBukry

$fNCAI TUFFS (Band Ri'ciu J + + +NN9

CN 7,a,b

++ +
+ ~+

NN9
NN9

CN 7,a,b
CN 7.a.b:e. URCA TUFFS/j<:: ~~SARHA$EL TUffSCl)'<:(~Cl

1

BAZNA TUFFS

~:(
- ~
L&.l

Nannoplan kton Envirpmenf
zones

STRATIGRAPHICAL UNITE'S

AG£~

as shallow marine sandstones in marginal parts of the basin
whereas outer selfrnarls was deposit in central parts of thebasin.
The major reorganization of the Transylvanian Basinoccurred in the Mid-Miocene (New Styrian phase), when
the basin acquired its present configuration. This
reorganization is linked with the emplacement of the east
Carpathian nappes. Transgressive clastics, marls and tuffs
were deposited, followed by deep marine salt layers. The
basin fill history ends with the deposition of a rapidly
subsiding Mid-Late Miocene brackish clastic sequence withmany tuffs intercalations (Fig. 1).
,
The nannoplankton assemblages recorded in the rnarlsof the Dej Tuffs are assigned to the zone NN5 (i.e. the zone
with Sphenolothus heteromorphus). The Ocna DejuluiBeds, which comprises the evaporites with gypsum andsalt, belongs to the zone NN5 too.
The next level of volcanic tuffs is the Borsa-Apahida
Tuffs, which contain assemblages of nannoplankton
assigned to zone NN6. This level is followed by the H d reni
Tuffs, which are correlated to the NN7 zone, and by theGhiris Tuffs, which correspond to the NN8 zone. This levelis followed by the S rm sel, the Urea Tuffs, and the Sincai
Tuffs, which all are correlated to NN9 zone. It should be
noted, that a precise dating of the deposits overlying thesalt has been possible by the study of nannoplankton within
the volcanic tuffs. The nannoplankton assemblages
between the tuff layers contain huge amount of reworked
Late Cretaceous and Paleogene forms, but only few
Miocene specimens.

~ (Colina, Zau J~~~ GHIRI$ TUFFS f RotbtN,Gnnari) + + +HAD.iJVJ1 TUFFS.........

(Bwfa,Cara, Ocna 11~)
/CLOD BEDS
11 !J~{l~A~1f1:/ti(J4 TUFFS

+ +-+

++-+

( Ciceu- 6iurgefti Formation ,Podeni
I irnestane)~...."' ~
-le:
t:l

<..
4)

CN 6
CN 5b

n,B
Deepermarine~··OCNA DEJULUI BEDS
(Salt, Gypsum)
DEJ TUFFS

NNB
NN7

t

NN6

CN Sa

NNS

CN 3,4NNS

CN 3,413,6Lagonallevo.arie
Outer
shelf
116.6

75=======================

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

HIGH RESOLUTION BIOSTRATIGRAPHY OF THE AMAZON FAN
Naja Mikkelsen
ODP Leg 155 drilled 17 sites on the Amazon deep-see fan,to study the evolution of the fan structure and to obtainhigh resolution paleoceanographic and pa1eoclimate
records. The sites recorded not only glacial-interglacial
climate cycles but also massive debris flows which isbelieved are triggered by changes in sea level.
Biostratigraphy with additional evidence from magneto-,
acoustic-, and stable isotope-stratigraphy have been used
to reconstruct the stratigraphy of the Amazon Fan.
Planktonic forarninifera and calcareous nannofossils
provide useful agemarkersatapproximately6, 9, 11, 40, 85,
130, 260, and 460 ka. Despite drilling to depths of over 400
m no datable sediments were recovered older than 460 ka,
this reflects the overall high Amazon Fan sedimentation

rates. The sedimentation rates range from 5 cm/ka in the
Holocene sections to over 250 cm/ka in parts of the lastglacial. Sites 942 and 946 contain an exceptional Oxygen
Isotope Stage 5 with an average sedimentation rate of 80
cm/ka. The Amazon Fan sediments thus provide theopportunity to obtain paleoceanographic records with thesimilar resolution to the ice cores.
The relative abundance offorarninifera and calcareous
nannofossil have provided valuable information on surface
water productivity and deep water corrositivity. All theserecords suggest that both the western equatorial Atlantic
Ocean and the Amazon River were dramatically different
during the last glacial compared with the late Holocene.

A STUDY OF THE FORAMINIFERAL AND CALCAREOUS NANNOPLANKTONASSEMBLAGES OF CORE SAMPLES TAKEN FROM THE LAHAR- AFFECTEDPORTIONS OF THE SOUTH CHINA SEA IN ZAMBALES PROVINCE,
PHILIPPINES
Prise ilia J. Militante-Matias and Marietta M De Leon
Monday, 16.25
A two-year study of selected core samples collected fromthe South China Sea fronting the lahar-affected area of theZambales province has been commenced. The purpose of
the study is to determine the occurrence and distribution,and thus document the forarniniferal and calcareous
nannoplankton assemblages present prior to, and during
the Mount Pinatubo eruption in June 1991. Ten piston
cores dredged by the Philippine Mines and Geosciences
Bureau-Department ofEnvironment and Natural Resources(MGB-DENR) during their 1992 expedition were initiallyinvestigated for calcareous nannoplankton while five werestudied for forarninifera. Preliminary results reveal thepresence of generally abundant, moderately- to wellpreserved, low-diversity assemblages. of calcareous
nannoplankton and planktonic forarninifera in sediments
of mostly volcanic materials. Benthonic forarninifera are
likewise abundant but are more diverse.

CALCAREOUS NANNOFOSSILS (HAUTERIVIAN) FROM "AGUA DE LA MULA"SECTION, NEUQuEN PROVINCE, ARGENTINA
E. Mostajo, A. Concheyro, F D zquez

Poster session
Topics: Hauterlvlan, Argentina, Stratlgraphy

The "Agua de la Mula" section comprises a thicksedimentary sequence of the Agrio F orrnation, and it crops
out at 38°S and 70°W, northern area ofNeuquen Province,
Argentina. The Agrio Formation is composed by threemembers: the Lower Member with claystones andlimestones, sandstones of the Avile Member and the Upper
Member with grainstones and subordinated limestones.
Lower and Upper Members ofAgrio Formation containammonites, spores, pollen, dinoflagellates and a scarce
nanoflora; the lower Member provides the following
nannofossils: Micrantholithus hoschulzii, M obtusus,
Chiastozygus striatus, Zeugrhabdotus embergerii, and
Watznaueria spp. The Upper Member shows a more diverse

hoschulzii, M. obtusus, Watznaueria biporta,
Ellipsage/osphaera britannica, Z. embergerii,
Cruciellipsis cuvil/ieri, Cretarhabdus spp. and
Watznaueria spp.
On the basis of C. striatus and C. cuvil/ieri thenannoflora of Agrio Formation in "Agua de la Mula" isassigned to the Zone Chiastozygus striatus, early-late
Hauterivian. Chiastozygus striatus has its first record inthis section at 397 m from the base ofLower Member of theAgrio Fm. It first appeareance indicates the base of theearly Hauterivian (Taylor, 1982).
The presence of Crucie//ipsis cuvi//ieri confirm a latenannofossil association with nannoconids and cocoliths,

Hauterivian age for the sedimentites of the Upper Member

among them: Nannoconus globu/us. N. bucheri, M

of Agrio Formation in this area.

==========================76===========================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplanldon Research, 17, 2, 1995.

CALCAREOUS NANNOFOSSIL PALEOCEANOGRAPHY OF THE LOWERCRETACEOUS OF NORTHWEST EUROPE
Jorg Mutterlose
Wednesday, 10.45
The paleobiogeographic distribution patterns of calcareous
nannofloras are caused by the interaction of various
autecological factors. Their long term and short term
fluctuations in the boreal early Cretaceous are controlled
by sea-level changes, temperature and nutrients.
Short term fluctuations (clay - marl rhythms) arecontrolled by surface water temperature and nutrients. The
nannofossil associations of the pale, marly horizons areindicative of warm surface waters, probably poor in
nutrients. These warm water assemblages, which have ahigh diversity, consist of R. asper, Cretarhabdus spp.,
Nannoconus spp, Conusphaera andMicrantholithus spp.
The dark, clayey beds are considered to have been
deposited under cool , nutrient-rich surface waterconditions. B. constans, S. horticus, Coro//ithion are
included in this assemblage. These fluctuations occur atthe scale ofMilankovitch cycles (precession and obliquity).

Superimposed on the short term cycles are longer term
fluctuations (3rd and 2nd order cycles ofHaq et al. 1987)
which are controlled by sea-level · changes. Regressive
periods favour the evolution ofboreal and endemic species
under restricted conditions. These regressive periods are:the latest Berriasian, the late early Hauterivian, the mid late
Hauterivian and the Barremian. Moderate sea-levelhighstands, on the other hand, allowed tethyan nannofloras
to spread into NW Europe and boreal species to migratesouthwards. High stands can be postulated for: the earlylate Valanginian, the early Hauterivian, the mid Hauterivian,the late Hauterivian and the late Earl Barremian.
A major shift towards a more open oceanic regime in
NW Europe was marked by the early Aptian transgression.
Endemic species disappeared and calcareous nannofloras
became homogenised and cosmopolitan.

THE NANNOPLANKTON OF THE JASLO LIMESTONE HORIZONSAndras Nagymarosy
Uhlig (1883) recognized thin limestone horizons in the
Paleogene part of the monotonous flysch sequence of thePolish Outer Carpathians, which serve as important tools in
the lithostratigraphic subdivision of the several km thickturbiditic sequences. The" Jaslo Limestones" (in Ukrainia"Holovetz Horizon") occur in several tectonic units of the
Carpathians, as the Dukla, Silesian, Subsilesian, Skole,
Boryslav-Pokuty nappes. Nowak (1965) observed, thatthese limestone horizons are products of intensive
calcareous nannoplankton blooms. A further similar
Paleogene nannochalk horizon (Krhovsky 1981), theDyn6w Marl occurs in several structural units of the Outer
Carpathians, as well. While most field geologists deny, thatthe single Jas1o. Limestone horizons would be corelable
between different outcrops, others, like Haczewski (1989)
subdivide the Jaslo Limestones into discrete horizons with
their own specific sedimentology, well-correlable along
hundreds of km distances. The nannoplankton
investigations show an individual character of the single
nannochalk horizons.
Dynow Marl: This not-microlarninated horizon contains big masses of Reticulafenestra ornata MULLER, R.
tokodensis B.ALDI-BEKE and somewhat less Transversapantis latus MULLER and Transversopontis fibula
GHET A. The sporadic occurrence of Spheno/ithus
distentus MARTINI proves the NP 23 age of the Dyn6w
Marl. All members of this nannoplankton bloom seem to be
Paratethys-endemic. This is confirmed by the appearanceof the endemic mollusc species Cardium /ipoldi in the
Dyn6wMarl.
Tylawa Limestone: The microlaminated Tylawa

Limestone horizon contains Reticu/ofenestra ornata
MULLER in big masses together with rare specimens ofTransversopontis fibula GHETA. The age of this horizonis also NP 23.
Jaslo Limestone (in a strict sense): Microlaminatednannochalk, its lower part consisting of blooms of
Cyclicargo/ithus ex. aff. jloridanus (ROTH et HAY)BUKRY with less Reticu/ofonestra omata MULLER, in its
upper part consisting entirely of C. ex. aff. jlorioonus (ROTHet HAY) BUKRY. This latter species is similar in many
respects to Cyclicargolithus abisectus (MULLER) WISE.
The age of this horizons can be near to the NP 23/24
boundary.
Zagon Limestone: Slightly or not micro1arninatedhorizon with blooms of Cyclicargolithus ex. affjloridanus(ROTH et HAY) BUKRY and Reticu/ofenestra ornata
MULLER. In its upper part (in one locality) also a
Reticu/ofenestra /ockeri MULLER bloom has been
observed. Its age is NP 24.
Folusz Limestone: Slightly laminated horizon (only in
the Silesian structural unit). It is built up of blooms of
Braarudosphaera bigelowii (GRAN et BRAARUD)
DEFLANDRE, Pontosphaera multipara (KAMPTNER)
ROTH and Cyclicargo/ithus ex. aff. jloridanus (ROTH et
HAY) BUKRY. Its age is probably NP 24.
Detailed investigations helped to prove, that single
horizons of the Jaslo Limestones contain consistently thesame nannoplankton assemblages everywhere and theseare differing from the assemblages of the other horizons.
The nannofossil assemblages of the Dyn6w Marl and the
Tylawa and Zag6rz horizons show fluctuations in salinity.

77===========================

Journal of Nannoplankton Research, 17, 2, 1995.

Fig.l.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

OUTER CARPATIANS !POLAND)

s

N
50 km

-- .......................................... .
---.,..------- .
............................................
~~C.ef. florldanusj

li!P. multipara
foB. bigelowii

t R.loetlerl

t C. d. florldanlll
R. ornata}• C. ef. rtttrldai'IUIR.ornota

SKOLE

UHIT
•R. ernata; T. fibula•R.ornata ..t. t fibula~~•R.ef. tokodensis
T.lotusEill2 ~3 ~=:=::/d4~

r==::=::=l..
~I~~~

Key to Fi~c 1 : 1 - menilite chert, 2 - Dyn6w Marl, 3 - dysodile shale, 4 - Kliwa Sandstone, 5 LoWer Krosno Fm., 6- Middle Krosno Pm., 7- UP.per Krosno Fm., 8- "Jaslo Limestone"
horizons, • - calcareous nannoplankton blooms (modified after Haczewski 1989)
Figure 1.: I - menilite chert, 2 - Dyn6w Mar!, 3 - dysodile shale, 4 - Kliwa Sandstone, 5 - Lower Krosno Fm., 6 - Middle Krosno Fm.,
7-Upper Krosno Fm., 8 - "Jaslo Limestone" horizons, * - calcareous nannoplanlcton blooms (modified after Haczewski 1989)

REFERENCES
Haczewski, G. (1989): Poziomy wapieni kokkolitowych w
serii menilitowo-krosnienskiej - rozr6znianie, korelacja igeneza (Coccolith limestone horizons in the MeniliteKrosno series, /Oiigocene, Carpathians/: Identification,correlation and origin). -Ann. Soc. Gool. Pol., 59,3-4,435-505
Krhovsky, J. (1981): Microbiostratigraphic correlations in theOuter Flysch Units of the Southern Moravia and influence of the eustacy on their paleogeographical development.- Zemni Plyn i Nafta, XXVI., Hodonin, 4.,665-688.

Nowak, W. (1965): Sur l'origine organique des calcaires deJaslo des couches menilitiques et de Krosno dans les
karpates flyscheuses (Oiigocene). - in: Carpatho-Balkan
Geol. Ass., Vll Congr., Reports, part 2, 1, 287-290.
Nowak, W., Geroch, S., Gasinski, A. (1985): Oligocene/
Miocene boundary in the Carpathians. - VIIIth Congr. Reg.
Corn. Medit. Neogene Strat., Abstracts, Hung. Geol. Surv.,
427-429.
Uhlig, V. (1983): Beitrllge zur Geologie der Westgalizischen
Karpathen. - Jb. k.u.k. Geol. Reichsanst., 33, 443-562.

CALCAREOUS NANNOPLANKTON BIOSTRATIGRAPHY OF THE SALZGITTERSALDER LIMESTONE QUARRY, LOWER SAXONY, GERMANY
F. Naji
Wednesday, 10.20

The SaJzgitter-Salder Limestone Quarry was proposed by
Wood et al. (1984) as an international standard section of
the Turonian- Coniacian stage boundary. They studied
the inoceramids and recommended that the base ofConiacian should be drawn at the level of the firstoccurrence of Cremnoceramus? walterdorfensis
hannovrensis, coincident with the Didymotis ecoevent 11.

Ammonites data of this section was reported by Kaplan
et al. ( 1987). Forresteria petrocoriensis was not recovered.
According to the ammonite stratigraphers the first
appearance of F. petrocoriensis represent the base ofConiacian.
Rich and diverse nannoplankton assemblages wererecovered including Quadrum gartneri, Eiffellithus

78==========================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

eximius, Lithastrinus septenarius, Lucianorhabdus
maleformis and Marthasterites furcatus . The firstoccurrence of M furcatus lies at the base of the marllayer
ME, which falls within the ammonite zone Subprionocyclus
neptuni of Early Late Turonian age. ME lies about 100 m
below the first occurrence of Cremnoceramus?
walterdorfensis hannovrensis and Didymotis ecoevent 11.
The discrepancies between the biostratigraphy bymeans of nannoplankton, ammonites and inocerarnids are
discussed.

Journal of Nannoplankton Resea.t:ch, 17, 2, 1995.

REFERENCES
Kaplan, U ., Kennedy, W .J . and Wright, C .W. 1987 :Turonian and Coniacian Scaphitidae from England andNorth-Western Germany. Geol. Jb. A 103: 5-39, Hannover.
Wood, C.J., Ernst, G. and Raseman, G. 1984: The TuronianConiacian stage boundary in Lower Saxony (Germany)
and adjacent areas: The Salzgitter-Salder Quarry as aproposed international standard section. Bull. Geoi.Soc.
Denmark 33: 225-238, Copenhagen.

FLORISTIC AND ISOTOPIC CHANGES AT THE PALEOCENE-EOCENE
BOUNDARY IN SLOVENIA
Jernej Pavsic and Tadej Dolenec
Poster session
A continuous transition between Paleocene and Eocene
was established on the ground of changes innannoplankton association in flysch at Nozno in Goricka
Brda, SW Slovenia. Nannoplankton in marls is rather
abundant but poorly preserved. Owing to high degree ofreworking of nannoliths for stratigraphy only species thatappearing in Eocene could be used. Reliably Eocene isonly the species Tribrachiatus bramlettei, along with someothers less important for boundary.
Across the boundary there are no sedimentation changes.
In Paleocene taken place normal flysch deposition withcarbonate turbidites that contain in base coarse grained
breccia. Upwards follow sandstone and in the uppermost
part grey marl (called opoka). In-between occurs fastinterbedding of marl and sandstone. Eocene starts with

i Ii
r1t

carbonate turbidite about 20 metres thick. Therefore no. samples for nannoplankton studies could be collected fromthis interval. Sampled was only the grey marl above twbidite
The isotopic composition of oxygen and carbon at thetransition from Paleocene to Eocene changes perceptibly
by increase of the sediment with rare oxygen and carbon
isotopes. The variability of isotopic composition of oxygenand carbon is most probably the result of temperature andclimatic variations that caused also changes in the carbon
cycle. Based on results of investigations in the beginningof Eocene somewhat colder conditions than in Upper
Paleocene are indicated. This probably caused the decreaseof organic carbon production, as confirmed by the jump of
the 8 13 C from negative values (- 4. 95o/oo) to positive values(+ 1.6696o).

r

IIIlll
i
II

1

I

I

... •iJ?:.:"i\:}
.....
·

181 •

.-.:::.:_:-_::.--:~-:::.::_;~~

V '\I''>~ A b,~~:V~~~ :an11H!
Jl I J 1
JJ- - -------·· ~- .. I I I I I I
Pc ~= .,.~~.:::::--;:- ~:·:
...
... I
E

......
107

...

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E

\
E

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ii

iii

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Figure 1: Litho logical section of the Paleocene-Eocene flysch interval and compilation of carbonate oxygen and carbon isotope data.

79

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995.

MORPHOMETRIC AND BIOCHRONOLOGIC STUDY OF
COCCOLITHUS MIOPELAGICUS
Alyssa Peleo-Aiampay
Poster session
Coccolithus miopelagicus is among the most cosmopolitan
species. Its last occurrence can potentially offer a valuable
datum for global stratigraphic correlations of Miocene
sediments. This could be especially useful in the highlatitudes where most standard index species are either rareor absent. As C. miopelagicus appears to differ from C.
pelagicus mainly by size and the latter species persists tothe present, it is important to make detailed size
measurements of this group and determine whether C.
miopelagicus is a distinct species that can be used inbiostratigraphy. It is also important to establish the age ofthis potential stratigraphic marker by correlation withmagnetostratigraphy at various sites.

Detailed morphometric and magneto-biochronologic
study of C. miopelagicus has been carried out at 8 DSDP I
ODP sites from low through high latitudes in bothhemispheres. The size definition for the total placolith
length(> 13 microns) for C. miopelagicus has proven to bea reliable criteria for differentiating this species from theother C. pelagicus complex species. Its last occurrence
consistently correlates with the lower part of magnetic
Chron C5n, with anageofl0.6-10.8 Main the low to midlatitudes (DSDP/ODP Sites 563, 845, 588 and 608). The
species is generally less abundant in the Southern
Hemisphere. At high southern latitude Sites 744 and 747,
the last occurrence of the species is earlier, correlating with
C5r(-11.7 Ma) at Site 744 and C5An (-12.3 Ma)at Site 747.

CALCAREOUS NANNOFOSSILS, TSUNAMITES AND THE Kff BOUNDARYOF NORTHEASTERN MEXICOJames J Pospichal
Tuesday, 11.35 and poster session

Calcareous nannofossils from closely-spaced samples acrossthe Cretaceous/Tertiary (KIT) boundary-from the Arroyo
el Mimbral and el Mulato sections in northeastern Mexico
were examined in order to determine the nannofossil
biostratigraphy and extinction patterns. In particular, theobjectives were to note the relationship of nannofossil
abundance of assemblage changes to unique clastic
sediments that mark the KIT boundary at these localities.
In general, the Mexican outcrops are comprised of upper
Maastrichtian greenish-grey marly pelagic limestones ofthe Mendez Formation and pelagic shales and marlstones
oflower Paleocene Velasco Formation. These pelagic units
are separated by a distinct, 1-3 m-thick, spherule-bearing,layered clastic bed, the origin of which, has been the subject
to much debate. The controversial clastic sediments havebeen attributed either to deposition by mega-tsunami
generated by the KIT impact nearby on the Yucatan
Peninsula, or conversely, to normal turbidite deposition
with no relation to the purported KIT impact.
The clastic sediments are divided into three subunits:
The lower subunit, or "spherule bed" (up to 1 m thick at
Mimbral), contains altered glass (tektites and microtektites),
shocked quartz, and common Mendez marl clasts. The
overlying sandstone subunit (up to 2 m thick) is gradedwith horizontal laminae and low-angle cross laminae. Plant
debris and Mendez clasts are present near the base of thissubunit. The top subunit (1 0-20 cm thick) consists of silts
and sands with distinctive rippled layers. Peak iridium
abundance has been noted in the upper part of this layer.
Above this subunit is a thin (up to 10 cm) layer oflimestonethat is overlain by shales of the Velasco Formation. The
consideration of this limestone layer as either lowermost
Danian or uppermost Maastrichtian is a debatable topic

and one that bears heavily on the interpretations of timing
and origin of the controversial clastic unit.
Calcareous nannofossils from the topmost 3 m of theMendez Formation at Mimbral and the topmost 1. 5 m at
Mulato are common to abundant and moderate to poorly
preserved. Nannofossil assemblages there belong to theupper MaastrichtianMicu/a princii Zone. Micu/a princii
is very rare along with few M murus and Lithraphidites
quadratus. Watznaueria barnesau, M decussata, andPrediscosphaera cretacea are the dominant componentsof the assemblage. Overall diversity of the uppermost
Maastrichtian assemblage at both localities is due to thegenerally poor preservation.
The clastic unit and the portion oflowermost Velasco
Formation studied at both Mimbral and Mulato belong to
the lowermost Danian Zone NPl. As expected, nannofossil
abundance drops considerably in the "spherule bed" andin the overlying sandstone units. In the shales andmarlstones of the Velasco Formation above, Cretaceous
specimens are few to common, but not as abundant as in
the underlying Mendez Formation. At Mimbral, marlstone
intraclasts from the "spherule bed" and the subunit above
contain abundant uppermost Maastrichtian nannofossils.
Only 2.5 m of the Velasco is exposed at Mimbral andnannofossil preservation in this interval is generally poor.
Preservation in the lowermost Velasco Formation is betterat Mulato and samples were analyzed from up to 6 m above
the top of the clastic unit. A slight increase inThoracosphaera is noted at the base ofVelasco Formation
just above the top of the clastic unit at both localities, andat Mulato, Braarudosphara bigelowii and B. alta arecommon starting 1 m above the clastic unit. At Mulato, thesurvivor assemblage also includes rare to few Chiastozygus

so========================~

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

ultimus, Cyc/agelosphaera reinhardtii, C. alta,
Zygodiscus sigmoides, Marka/ius inversus and Octolithus
mu/tip/us. The first Danian species to appear at either
locality, Neobiscutum parvulum, first occurs at I m above
the top of the clastic unit at Mimbral and 25 cm above theclastic unit at Mulato. Cruciplacolithus primus first occur
about 5 m above the top of the clastic unit at the latter site.
Nannofossil assemblages are interpreted to indicate that
the Kff boundary should be placed at the base of the"spherule bed", contrary to some previous interpretations
in which the boundary is located at the top of the clastic
unit. This is suggested by the drop in abundance ofCretaceous specimens at the base of the "spherule bed"
along with the observation that Cretaceous specimen
abundance does not recover above the clastic unit. Notably,
this includes abundances within the limestone layer that

Journal of Nannoplankton Research, 17, 2, 1995.

immediately overlies the clastic beds. The few to common
Cretaceous nannofossils present in basal Velasco areprobably reworked as are those present within the clastic
unit. In addition, upper Campanian-lower Maastrichtian
species are more conspicuous in the Velasco sediments
above the clastic unit, which also indicates persistent
reworking.
Overall, the study indicates that Cretaceous
nannoplankton suffered a rapid reduction at the Kff
boundary (marked by the clastic unit) and never recovered
following the deposition of the spherule sandstone units.
This perhaps suggests a fundamental link between endCretaceous nannoplankton extinctions and the event(s)associated with the deposition of the unique clastic
sediments in northeastern Mexico.

CALCAREOUS NANNOFOSSILS AND PALYNOMORPHS FROM VALANGINIAN
AND HAUTERIVIAN (LOWER CRETACEOUS) STRATA OF CERRO DE LA
PARVA, CENTRAL- WESTERN NEUQUEN, ARGENTINA
M Pramparo, W Volkheimer, and E. Mostajo
Poster session
At Cerro de la Parva locality are outcropping pelites andpsammites of the Valanginian Mulichinco Formation (withthe ammonite Olcostephanus atherstoni of Upper
Valanginia.Q age, which occurs in the upper part of theFormation) and pelites of the Lower Member of Agrio
Formation (Hauterivian). A detailed sampling fornannofossils and palynomorphs has been carried out inboth mentioned stratigraphic units. The following species
could be identified:
1) Nannofossils:a) Mulichinco Formation: Watznaueria barnesae,

Watznaueria britannica, Cyclagelosphaera margerelii, Micrantholithus hoschulzii, Micrantholithus
obtusus, Calcicalathina oblongata, Zeugrhabdotus
embergeri, Nannoconus steinmannii, Nannoconus steinmannii minor, Watznaueria sp. and Rucinolithus sp.
b) Agrio Formation (Lower Member): Watznaueria
barnesae, Watznaueria britannica, Cyclagelosphaera
margerelii, Micrantholithus obtusus, Micrantholithus
hoschulzii, Zeugrhabdotus embergeri, Crucie/lipsis
cuvillieri, Cretarhabdus surirellus, Nannoconus
steinmannii, Nannoconus cornuta, N. globulus, N.

bucheri, N. kamptneri, N. broennimannii, Watznaueriasp., Chiastozygus sp. and Nannoconus sp ..
2) Palynomorphs:a) Mulichinco Formation: The assemblage ischaracterized mainly by terrestrial species: Balmeiopsis

limbatus, Cal/iaslasporites turbatus, Ca/lialasporites
dampieri, Podocarpidites ellipticus, Microcachrydites
antarticus, Equisetosporites caichiguensis, C/assopollis
simplex. A few marine species are present~ Cribroperidin!um orthoceras, Muderongia sp., Cymatiosphaera
sp. and Baltisphaeridium sp ..
b) Agrio Formation (Lower Member): In this part of thesequence marine species are more frequent; amongst themdominate:
0/igosphaeridium
cf.
complex,
Cribroperidinium orthoceras, Sentusidinium sp.,
Pareodinia sp., Gonyaulacysta sp., Pterospermel/a sp.,
Muderongia sp., Escharisphaeridia pocockii,
Leiosphaeridia spp. Prominent terrestrial forms are:Deltoidospora sp., Biretisporites sp., Cyc/usphaera psilata(very frequent), Araucariacites austra/is, Cal/ialasporites

dampieri, Cal/ialasporites trilobatus, Classopo/lis
simplex and Podocarpidites sp.

PALEOECOLOGY OF CALCAREOUS NANNOFOSSIL ASSEMBLAGES AND ITSRELATIONSHIP TO SEA- LEVEL VARIATIONS IN THE FIGOLS GROUP(EARLY EOCENE, SPANISH PYRENEES)
Viviana Rea/e
Tuesday, 10.45

Sea-level fluctuations are a detennining factor in influencing
ecological conditions of shelfal settings. Little is known
about the relationships between such changes and theabundance and diversity of calcareous nannofossils. If sealevel changes can be documented thanks to the study ofdepositional sequences (Vail et al. 1991 ), then it seems of=========================81

overall importance that paleocological studies be tied to awell-known sequence stratigraphic framework. These
conditions are met in the Early Eocene Figols Group of the
Spanish Pyrenees (Tremp-Garus Basin) studied by Mutti etal. (1988;1994) and carminani (1992). Here a high-re&>lution
framework has been made available through extensive

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

facies analyses carried out along a 25 km-long stratigraphic
cross-section numing in an onshore-offshore direction, fromshallow water to distal shelf settings (Carminatti, 1992). The
Figols Group spans between the Zone NP11 and the NP12
(R.eale 1994). It is composed offour Large Scale Composite
Depositional Sequences (LSCDSs, nained FG 1-4, Mutti etal., 1994) which are the product of third-order sea-levelvariations. These are in turn composed of Elementary
Depositional Sequences (EDS), 20-200 m thick, producedby high-frequency sea-level changes (fourth and fifth
order). The maximum thickness of the Figols Group in the
study area is about 1200 m.
A quantitative analysis of calcareous nannofossil
assemblages has been carried out on three sections
outcropping between Esera and lsabena Valleys: Merli Est,
Teraza and Navarri, from proximal to distal. The results will
be discussed from two different points of views, the firstregarding the distribution of abundance and diversities atlarge scale (group), the second at a small scale (EDS).
1) The study of the distribution of taxa of "shallow
water" affinity (pentaliths, Rhabdosphaera, Rhomboaster,T. ortostylus) shows asharp increase in the upper part of
the group. It coincides with sequences FG3 and FG4 whichmark a basin narrowing and a decrease ofbathymetry.
Spheno/ithus and Z. bijugatus show opposite trends,
the first being maximum during the main transgressive partof the group (FG2).
The quantitative analysis of reworked taxa (mainly
Creataceous) shows that reworking is greatest during theregressive part of the group.
A study of diversity offossil assemblages has been also
performed. Species richness, Shannon-Weaver Index andEquitability have been calculated. The highest values areagain concomitant with the deposition ofFG3 and FG4.
2) A cyclic trend correlative to EDSs development andhigh-frequency sea-level changes is clear in the distributionof reworked taxa along the succession. Reworking has thehighest value during highstands and the lowest during thetransgressive intervals.
REFERENCES
Carminatti M. 1992: Stratigrafia fisica e modellizzazione
sismica inversa del Gruppo di Figols affiorante tra la Val
Isabena e la Val Esera (Pirenei) . Tesi di Dottorato in
Scienze della Terra. Universitf di Parma, Italy.
Mutti E ., Seguret M., Sgavetti M. 1988: Sedimentation anddeformation in the Tertiary sequences of the Southern
Pyrenees. In : A.A.P.G. Mediterranean Basin Conference,Spec.Pubbl., Field Trip n.7.
Mutti E., Sgavetti M., Waehry A., Carminatti M. Davoli G.,
Ghielmi M., Figoni M. and Mora S. 1994: Regional
stratigraphy and sequence -stratigraphic aspects of the
Figols Group. In: Mutti et al. (eds) The Eastern Sectorof the South-Central for Stratigra:phic Analysis andExcursion Notes. Second High-Resolution SequenceStratigraphy Conference, 20-26 June 1994, Tremp,
Catalunya, Spain.
Reale V. 1994: Biostratigrafia e Paleoecologia a nannofossili
calcarei del Gruppo di Figols, Eocene lnferiore (Bacinodi Tremp-Pamplona, Spagna). Tesi di Dottorato in
Paleontologia. Universitf di Modena, Italy.
Vail P.R., Audemard S.A. Bowman P.N. Eisner and G. PerezCruz 1991: The stratigraphic signature of tectonics,
eustasy and sedimentation. In: Einsele G. et al. (eds),
Cycles and event in stratigraphy.

CALCAREOUS NANNOPLANKTON FROM THE BOUNDARY DEPOSITS OF
MAASTRICHTIAN AND DANIAN OF THE UKRAINIAN CARPATHIANS
Anna Romaniv
Poster session
Calcareous nannoplankton on the boundaries ofMaastrichtian and Danian was studied within the northernand southern hillsides of the Ukrainian Carpathians.
The upper Cretaceous and Paleocene deposits
considerably occur in the Carpathians. They are presented
by rather monotonous terrigenic flysch. Gradual transition
from Maastrichtian to Paleocenic deposits is observed, and
it is difficult to establish the boundary between them under
the field investigations. Nowadays it is possible to prove
the presence ofDanian stage in some sections by means of
microfauna (Vialov et al., 1960; 1965) and by narmoplankton(Grigorovich, 1971; Romaniv, 1991).
Calcareous nannoplankton of Maastrichtian deposits
has rich quantitative and species content. It numbers about
60 species which occur in 28 genera and 8 families. The
families Zygodiscadeae Hay et Mohler, Coccolithacaea
Kamptner and Syracosphaeraceae Lemmermann arepresented by the majority of genera. Among the mostcharacteristic genera we should noteMarkalius nielsenae,

Nephrolithus frequens,
Broinsoinia parco,
Cribrospaerella ehrenbergi, Kamptnerius magni.ficus,

Micula concava, M. staurophora, Predeiscophaera
cretacea, Tetralithus acu/eus, Titrifidus. Tetrat/ithus

murus can be observed in some sections.
On the boundary of Maastrichtian Danian significant
changes in content offossil assemblages take place. Theircontent is almost totally renewed taking Paleocenic features.
Danian nannofossils are less different by their species
content and they number not more than 20 species. Zones
NP 1 Marka/ius inversus, NP.2 Crucip/aco/ithus tenuis
and NP 3 Chiasmo/ithus danicus have been noticed in
Danian of the Carpathians.
REFERENCES
Vialov O.S., Dabagian N.V., Kulchytskiy Ya. 0., 1960: 0
granitse mezhdu melom i paleogenom v Vostochnych Karpatach. Granitsy melovych i tetrichnych otlozheniy, 105-122.
Vialov O.S., Dabagian N.V., Kulchytskiy Ya.O., 1965: Pro
datskiy yarus i granytsu paleogenu v Schidnych Karpatach. Geologichny zhurnal, tom XXV, vup. 4, 118~119 .
Grigorovich A.S. 1971: Microfitoplankton melovych ipaleogenovych otlozheniy severnogo sklona Ukrainskich Karpat. B ulleten Moskovskogo obshchestva
ispytateley prirody, otdel geologicheskiy, 2, 83-98 .
Romaniv A.M. 1991: Izvestkoviy nanoplanlcton melovych
i paleogenovych otlozhneniy Ukrainskich Karpat, 166s.

82==========================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995.

NANNOFOS~ILS AND PLANKTIC FORAMINIFERA ACROSS THE Kff

BOUNDARY IN TWO SECTIONS OF NORTHEASTERN MEXICO
Antonieta Sanchez-Rios, Hector Ruiz-Ruiz, Patricia Padilla, and J. Manuel Grajales-Nishimura

Poster session
Floristic and faunistic changes in calcareous
nannoplankton (CN) and planktic forarninifera (PF) wereobserved through the Cretaceousffertiary boundary fromthe Lajilla and Coxquihui sections, NE Tamaulipas and NE
Veracruz states, respectively.
Three lithologic .units can be distinguished in both
sections: Unit I (uppermost Mendez Formation) is
composed by marls; Unit 11 (clastic unit) contains tektites,
cross-bedded and parallel-bedded sand-stones, siltstones,
and rare reworked limestone clasts; Unit Ill (basal Velasco
Formation) is formed by marls, calcareous shales, and clayey
limestones.
Unitl (Lajilla = 1.20 m, Coxquihui =3.45 m thick). At theLajilla section, 38 CN and 55 PF species were identified,
whereas at Coxquihui these abundances correspond to 37
and 80, respectively. Moderate preservation of fossils isshown at both localities, where both uppermost
Maastrichtian species Micula prinsii andAbathomphalus
mayaroensis were found.
Unit 11 (Lajilla = 1.1 m, Coxquihui = 0.80 m thick).

Compared to Unit 11, Cretaceous PF abundance decreases
around 60%, and that ofCN does it at 50%. M prinsii isabsent at b(>th sections and A . mayaroensis continues onlyat La Lajilla; at this latter section, scarce "small globigerina"
appear at the top of this unit.
Unit lli (Lajilla = 2.80 m, Coxquihui = 1.60 m thick). In
contrast with the 80 PF species from the Unit I at Coxquihui,
only 30 were found in the Unit Ill, crossing the Kff
boundary; by the other hand, only 16 out of 55 wereregistered at La Lajilla. Both Biantholithus sparsus FAD
and the Thoracosphaera "bloom" are detected at the baseof this unit; one meter above, the Braarudosphaera
bigelowi "bloom" was identified; at La Lajilla, Neobiscutum
cf. parvulum is present. In both localities the firstoccurrence of the Early Paleocene Parvolarugoglobigerina eugubina is registered at this level.
Both sections share good chronostratigraphic
correlation; the Kff boundary was placed between the
Unit 11 and Ill.

LATE PLIOCENE NANNOFOSSIL EVENTS RECOGNIZED IN THE UPPERMOSTSEQUENCE IN THE JAPAN SEA SIDE, WITH REFERENCE TO THE
GLACIATION IN THE ARCTIC SEATokiyuki Sato and Koji Kameo

Poster session
The remarkable floral change ofthe calcareous nannofossils
from Reticulofenestra spp.(small form) assemblage to
Coccolithus pelagicus assemblage, is found in the Upper
Pliocene sequence in Akita area, located in the Japan sea
side of Japan. This event is correlated to the latest Gauss
Normal Epoch. The relation between the magnetic polarity
and the nannofossil event is al~ found in the Upper

Pliocene of Hole 911 A, ODP Leg 151, and is correlated tothe horizon of the drastic increase of dropstones, which isrelated to glaciation of the northern hemisphere. These
results indicate that calcareous nannofossil event
recognized in Upper Pliocene in the Japan Sea side isstrongly related to the increase of ice sheets in the northernhemisphere occurs at latest Gauss Normal Epoch.

LATE CRETACEOUS BIOSTRATIGRAPHY AND PALEOCEANOGRAPHY
OF THE ATLANTIC COASTAL PLAINS, USA
Jean Self-Trail

Wednesday, 9.15
Subsurface Upper Cretaceous marine sediments from nine
coreholes in South Carolina, one corehole in northern North
Carolina, one corehole in central Delaware, and four
coreholes in southern New Jersey were examined for
calcareous nannofossils using the light microscope and thescanning electron microscope. Correlation oflithologic units
across state boundaries is possible on the basis of thecalcareous nannofossil biostratigraphic data.
Biostratigraphic ages ofthe lithologic units remain fairly
constant from north to south. In New Jersey, ages of marine
sediments range from latest Cenomanian (Zone CC lOb) for
the Bass River Formation to late Maastrichtian (Zone CC26a) for the NavesinkFormation. Marine sediments in South
Carolina, Delaware, and probably North Carolina range inage from the Santonian (Zone CC 15) to the late
Maastrichtian (Zone CC 25). Latest Cenomanian and latest
Maastrichtian marine units have not been documented inthese three states. Cenomanian marine sediments, which
do occur in New Jersey, are rare throughout much of theAtlantic coastal plain. There is a regional unconforrnity
documented in all four states between the top of Zone CC
22 (probable top of the Campanian) and the base of Zone
CC 25 (lower to middle Maastrichtian).
Calcareous nannofossils document possible changes

83Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

in the position of the Gulf Stream current during theCampanian and Maastrichtian. Quadrum trijidum andQuadrum sissinghii are rare in New Jersey, with only one
specimen of each species found in each of the four cores
examined. This is remarkable when compared to South
Carolina, where both species are very abundant. Differencesin the abundances of these two species between the more
subtropical area (South Carolina) and the more tempemte
area (New Jersey) reflect the position of the Gulf Stream.

During the Late Cretaceous, Quadrum sissinghii and Q.
trijidum preferred the warmer waters of the South Atlantic
and Gulf Stream to the cooler waters found off New Jersey
and Delaware. Nephrolithus frequens, which first appears
in the Campanian in high-latitude waters and in the
Maastrichtian in more temperate waters, is absent in South
Carolina but common in New Jersey. It's appearance orabsence also is thought to be related to the position of thewarm-water Gulf Stream.

PALEOGENE AND NEOGENE PRODUCTIVITY IN THE INDIAN OCEAN
William G. Siesser
Poster session
Primary productivity in the oceans is an important processwith ramifications for biological, geological, and chemical
oceanography. Productivity removes enormous amountsof carbon and smaller amounts ofother elements from ocean
waters. Vast quantities ofthese elements eventually become
locked away in sediments on the sea floor and in onshore
deposits that originally formed in ancient oceans. The
geological record of the carbon system is thus important inunderstanding global change.
Paleoproductivity in the oligotrophic areas of the world's
oceans has been investigated less than in the more fertilenearshore areas, in part because of the absence of a reliable
proxy to measure productivity in oligotrophic areas. A
transfer function has recently been proposed which directlytranslates carbonate mass accumulation rates into aquantitative measure of productivity. This transfer function
has been applied at six ODP sites in the oligotrophic Indian
Ocean in order to investigate temporal and spatial changes

in Indian Ocean productivity during the Tertiary Period.
Early Paleogene productivity in the Indian Ocean wasconsiderably higher than in the late Paleogene and
Neogene. A warmer, more confined sea, with large riverine
nutrient input from close lying land masses may accountfor the generally higher early Paleogene productivity.
Productivity increased sharply during Paleocene
nannofossil Zone NP 5 and during Eocene Zone NP 11.
These productivity peaks may be related to abrupt climaticchanges which reorganized oceanic circulation andstimulated major changes in productivity. Global coolingand the initiation of the modem Indian Ocean circulation
system caused productivity to decrease in the Oligocene.
This trend continued into the Neogene, which wascharacterized by generally low productivity, interspersedwith occasionally higher productivity levels, especially at
the more northern sites in the Indian Ocean.

DEVELOPMENT OF THE PLIO- PLEISTOCENE COCCOLITH ASSEMBLAGESIN THE NE ATLANTIC CORRELATED TO CLIMATIC CHANGESXin SuMonday, 12.25
A quantitative study of Plio'-Pleistocene calcareous
nannoplankton of the DSDP/ODP sites 664, 659 608,609,
610 from the Northeast Atlantic was carried out to evaluate
the development of the coccolith assemblages under the
ecological impact of climatic changes during the last 5.2
my.
The main results of this study are:
1. Vario~s species of Reticulofenestra andGephyrocapsa, Pseudoemiliania /acunosa andEmiliania
huxleyi are the main components of the coccolithassemblages. Major evolutionary processes in these species
are recognized by downcore variations in their accumulation
rates. The decline and extin~on ofMiocene forms, i.e most
Reticulofenestra species, and two genera Discoaster andSphenolithus, and the appearance and increase ofPliocene
and Pleistocene species, especially the evolutionarychanges within Gephyrocapsa, are seen as the main
mechanisms of the development of the coccolithassemblages.

2. Eight developmental stages of the coccolithassemblages are distinguished on the base of fundamental
changes in their essential components:
Coccolith assemblages in the Pliocene stages are
dominated by Reticulofenestra species and those in the
Pleistocene stages are characterized by frequently
alternating dominances of Gephyrocapsa species and P.
lacunosa. Today, E. huxleyi is the dominant species. In
the Pleistocene changes in the dominant species are more
rapid and abrupt than in the Pliocene.
The coccolith assemblages show a variety ofgeographical variations throughout the eight stages, which
are caused by the various ecological affinities of these
species. For example in tlie Early Pliocene Discoaster spp.
and Sphenolithus spp. are common in low latitudes andrare in high latitudes; in the late Pleistocene (0.60- 0.25
Ma) Gephyrocapsa oceanica and G. margereli areabundant in low latitudes whereas G. caribbeanica isprominent in high latitudes.

84===========================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

3. In order to make a link of climatic changes and thecoccolith development, a statistical method (CV ratio) is
introduced to analyze the variability of the benthic 8 1SO
data at site 659 (Tiedemann et al., 1994) and ofaccumulation
rates (ARcoccoliths) of six coccolith species from the fivestudied sites and. Generally, the 8 1SO CV ratios reflect thevariability of temperatures/ice-volumes or climatic changes
and the ARcoccoliths CV ratios of a species are related to
the variability of its production levels, which is the resultsof climatically induced changes in marine ecosystem, aschanges in temperatures and light.
For the most time intervals the ARcoccoliths CV ratio
curves of most species show a good correlation to the 8 1SO
curve. In the Pliocene low ARcoccoliths CV ratios parallel
low 8u10 CV ratios, this indicates that coccolith species
showed small variations in production within stable climaticconditions. In the Pleistocene strongly increased 8 1SO CV
ratios are parallelled by strongly increased ARcoccoliths

Journal ofNannoplankton Research, 17, 2, 1995.

CV ratios, this suggests that coccolith species showed largeamplitude variations in production, in response to increased
climatic instability due to frequent glacial-interglacial
alternations. The extinction rates of species increase in the
Pleistocene when 8 1SO CV ratios increase. Titis implies thatthe strongly increased climatic instability in the Pleistocene
may lead to the extinction of more species. Thus, the rapid
and abrupt changes of the coccolith assemblages in the
Pleistocene are correlated with increased climatic instability.
However, the ARcoccoliths CV ratios in several
intervals, e.x near the appearance of a species (e.g. G.
oceanica) or the intervals where certain changes in theirecological affinities are observed, do not parallel the 8 1SO
CV ratios and the appearance rates of species are not inparallel with the 8 1SO CV ratios. This indicates that thevariations in abundances which are induced by biologicalevolution are not directly correlated with climatic changes.

RARE OCCURRENCES OF PETRARHABDUS COPULATUS DEFLANDRE
ON THE NORTHERN HEMISPHERE (CENTRAL EUROPE)
Lilian Swibeniclai
Poster session
Topics: Campanian, Central Europe, bioprovincu

l

NORTH
SEA
BASIN

'@
3

Q
...._ _250.._,-~St;XJ km
r-::-r:f~ AREAS UPLIFTED

BY~CONTINENTAL AREAS~ SUB-HERCYNIAN AND<:===WARM SURFACE CURRENTS~COlD BOTTOM CURRENTS

LARAMIAN TECTONICSMBMUNSTER lAND BASIN•

OCCURRENCES OF PETRARHABOUS COPULATUS

Figure 1. Paleogeography and water circulation in the late Upper Cretaceous of Central Europe (modified after Ziegler (1982) and Kaeverand Lommerzheim (1991)) with marked finds of Petrarhabdus copulatus Deflandre (hypothetic locations). l. Waschberg Zone, Low
Austria, 2 - Zdanice Unit, South Moravia.

=========================85

Journal of Nannoplankton Research, 17, 2, 199.5.

6th INA Conference, Copenhagen 199.5, Programme and Abstracts.

Petrarhabdus copulatus Deflandre is mostly known fromthe southern hemisphere in the Indian Ocean and Atlantic
Ocean being conunon in the Carnpanian and Maastrichtian
sediments of approximate paleotitudes 30° and 40°S but
absent from the samples of the same age from the morepoleward localities (Wind 1975). Finds of this species fromthe northern hemisphere are rarely mentioned in theliterature (i.e. Deflandre ( 1959) from the French
Maastrichtian sedirnents or Varol ( 1992) from Turkey) andmay prove the importance for the paleogeographicalreconstructions and further bioprovince studies.
Petrarhabdus copula/us has been recorded in the Late
Carnpanian sediments of the Outer Group of the nappes in
the West Carpathians (Zdamce Unit in the South Moravia,
Czech Republic) and in the Waschberg Zone in Low Austria
in the assemblages where mixing oflow- and high-latitude
nannofossil species was obvious (Svabenicka, in press).
These sediments were deposited east of their present
locations. Besides, this nannolith was observed also in thesediments of the Miinsterland Basin which is included into
the boreal bioprovince (NW Germany) and where typicallow- and mid-latitude nannofossils were absent.
Brief review of the Petrarhabdus copulatus
occurrences observed by the author:- Waschberg Zone (locality Emstbrunn): P. copulatus

accompanied by Quadrum trifidum, Q. sissinghii, Neocrepidolithus watkinsii, Biscutum coronum etc.
- Zdanice Unit (Carpathanian Flysch Belt, locality
Pavlov): P. copula/us in the association with Quadrum
sissinghii, Ceratolithoides arcuatus, Biscutum dissimilis,
B. coronum, Monomarginatus quaternarius, Prediscosphaera stoveri etc.
-MUnster Basin (borehole Longinusturm): P. copulatus
associated with Prediscosphaera stoveri, P. cf. grandis,
Neocrapidolithus watkinsii, Monomarginatus quaternarius, Micu/a swastica etc.
REFERENCES
Deflandre G. (1959): Sur les nannofossiles calcaires et leur"·systematique. - Rev. Micropaleontol., 2, 127-152. Paris.
Svabenicka L. (in press): The stratigraphical correlation of
the Campanian low- and high-latitude calcareous
nannofossils inSouthMoravia(the West
Carpathians). - Geologica Carpathica. Bratislava.
Varol 0 . (1992) : Taxonomic rev1s1on of the
Polycyclolithaceae and its contribution to Cretaceous
biostratigraphy. - Newsl. Stratigr., 27, 93-127. Berlin.
Wind F.H . (1975) : Tetralithus copulatus Deflandre(Coccolithophyceae) from the Indian Ocean: A possible
paleoecological indicator. - Antarct. J.U.S., 10, 265-268 .
Washington.

THE DANIAN (LOWER PALEOCENE) LIMESTONE DEPOSITS IN DENMARK:BASIN DEVELOPMENT AND SEQUENCE STRA TIGRAPHY
Erik Thomsen
Poster session

This overview of the Danian limestone deposits in Denmarkis based on biostratigraphical and lithological studies ofmore than 40 wells and a similar number of outcrops. The
biostratigraphical framework is based on calcareous
nannofossils. Nine nannofossil zones, which could be easily
identify in all sections, were recognized. The zonation is aslightly modified version of the zonation scheme presented
by Perch-Nielsen ( 1979). The deposits, which consists ofpure limestone were subdivided into three main facies:
Btyozoan limestone (mound forming limestone with morethan 20% btyozoans; calcilutite (chalk-like limestonecomposed of calcareous nannofossils and planktonic
foraminifera); and calcarenite (similar to the calcilutite butwith a higher proportion of sand-sized components.
The deposits can be subdivided into depositional units
on the basis of the occurrence of major hiati, the pattern of
onlap and offiap on structural highs, and the distributionof sedimentary facies. The units are considered to bedepositional sequences.
Four depositional sequences were recognized from theCretaceousffertiaiy boundary to the top of the Danian.
Important aspects of their of their distribution in time andspace are illustrated in the north-south profile shown infigure 1. It should be noted that the northern part of the
profile is missing due to post Danian uplift and erosion.
Sequence I (uppermost Cretaceous and lowermost
Danian) is confined to a narrow zone in the central part of==========================86

the Norwegian-Danish Basin. The sequence is subdivided
into two J?art by the boundary clay at the CretaceousTertiary boundary. The boundary event affected thelithology of the limestone, but did not otherwise influence
the development of the sequence. The top of the sequenceis nearly everywhere marked by a hardground and clear
evidence of erosion.
Sequence 2 (lower Danian) covers a much larger area
than sequence I. The deposits consists of mound forming
btyozoan limestone. The top of the sequence is marked bya hardground and extensive erosion.
Sequence 3. (MiddleDanian) Onlap on the RingkebingFyn High indicates a further expansion of the depositional
basin. The facies changes from btyozoan limestone to afine-grained pelagic calcilutite composed mainly of remainsof calcareous nannofossils. The boundary between
sequences 3 and 4 is marked by a hiatus and erosion in the
top of sequence 3 in the eastern part of the basin and on
the Ringkebing-Fyn High.
Sequence 4 is associated with an expansion of theDanian sea across the Ringkebing-FynHigh. This sequence
covers a much iarger area than any ofproceeding sequences.
The facies consists of pelagic calcilutite in the NorwegianDanishBasin and ofbtyozoan limestone on the RingkebingFyn High. During this period the northern margin of thebasin moved south due to an uplift of the Fennoscandian
Border Zone. The boundary between Danian and theSelandian is generally marked by a hiatus and erosion.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

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POLAR COCCOLITHOPHORIDS
Helge Abildhauge Thomsen
Monday, 14.50
The preparation of freshly collected samples for TEM has
resulted in the finding of a contingent oflightly calcified
coccolithophorids, which appear to have their main
distribution in polar regions. These organisms were firstencountered in subarctic and arctic samples and were later
found to form a characteristic nannoplanktonic element
also in Antarctic waters . Several taxa of polarcoccolithophorids previously considered to be autonomous
species are, in fact, part oflife histories combining hetero-87

and holococcolithophorid forms. All species of
Haptophyceae, with. the exception of the enigmatic
Balaniger balticus, have been considered photosynthetic.
However, it has become evident that all polarcoccolithophorids are in fact heterotrophic organisms. It
remains to be verified whether these taxa are genuine
heterotrophic organisms, or forms that have secondarily
lost the photosynthetic apparatus.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

CHANGES OF CALCAREOUS NANNOPLANKTON EVOLUTIONARY DIVERSITYDURING THE PALEOGENE
Mao/a Ushakova
Poster session

In the DSDP and ODP sediment cores the quantity ofextincted and appeared nannoplankton species and genera
was counted for the different Paleogene and Early Neogene
epochs.
The maximmn of the first appearance level (FAD) was
marked for Early Eocene. The maximum of the last
occurrence levels (LAD) was in the Late Eocene. Total
species and genera diversity was observed in the Middle
Eocene. The maximmn of genera FAD and LAD situated in

the same epoch. The relatively great nmnber of new genera
was noticed also in the latest Paleocene. The minimum of
nannoplanktonic species and genera, FAD and LAD andtotal diversity occurred in the Early Paleocene and in the
Late Oligocene- Early Miocene.
Thus the optimal environmental conditions of
nannoflora development prevailed in Middle Eocene andin the latest Paleocene. These results were confirmed by
the planktonic foraminifera and oxygen isotopic data.

UTILITY OF CALCAREOUS NANNOFOSSILS AND ORGANIC REMAINS: IN THE
RECONSTRUCTION OF THERMAL METAMORPHISM IN THE HATRURIM
FORMATION (TERTIARY, SOUTHERN ISRAEL)
S. Vo/in, Y. Eshet, and H. Kish

Poster session
The Hatrurim Formation occurs in synclines in central andsouthern Israel. It is composed of a mineralogical suite thatindicates a thermal metamorphism. It is generally suggested
that This unit formed from the thermal metamorphism ofCampanian-Maastrichtian organic-rich sequences thatwere combusted and burned, probably during the Tertiary.
The present research deals with the reconstruction of
combustion foci and the metamorphic halo in the marginsof the Hatrurim syncline, with a special emphasis on thereconstruction of the low-grade levels, before ametamorphic mineralogical suite forms. The optical andstructural changes in organic and calcareous-walledmicrofossils are used to characterize the low-grade
metamorphic changes. The methods used in this research
to define and reconstruct the metamorphic halo are:
1. Structural changes in calcareous nannofossils: themethod is based on the rate of elimination of calcareous
nannofossil taxa during the metamorphic process. The
following parameters from calcareous nannofossils are
utilized:- Species diversity: a gradual decrease in species
diversity with increasing m~tamorphism is observed, until
only nannofossil "ghosts" are left.
-Number of specimens: parallel to the decrease in species

diversity, a decrease in number of nannofossil specimens isobserved.
- Change in optical properties: this change is caused by
the re-organization that crystals undergo duringmetamorphism and results in the creation of new opticalfeatures of calcareous nannofossils.
2. Thermal Alteration Index (TAI): a method based on
the fact that organic matter in rocks (pollen, algae andspores) undergoes a process of darkening with theincreasing thermal alteration. It is calibrated to the vitrinitereflectance method and can be used to detect metamorphism
in low grade levels.
Preliminary results: Indications from the metamorphosed
microfossils suggest:
1. Metamorphic foci are small, in the range of I 0-40
meters.
2. Using microfossil remains, it is possible to distinguishbetween combustion that happened under aerobic
conditions, and combustion that occurred with a limited
oxygen supply.
3. Our results focus on the low-grade intervals of
metamorphism and are complementary to the metamorphic
mineralogical studies that focus on the higher grades. This
allows a better reconstruction of this thermal metamorphic
phenomenon in the Hatrurim Formation.

CALCAREOUS NANNOFOSSILS IN THE ARTS
Katharina von Sa/is
Wednesday, 14.00

Calcareous nannofossils have a long evolutionary history
which makes them important in dating marine sediments of
up to 200 million years of age. Since such rocks have beenused for the construction of houses and churches as well
as for grounds for paintings, the analyses offossil coccoliths
can also contribute to the solving of archaeological and art

historical riddles.

Thanks to the widespread occurrence of chalk - a
sediment widespread in Scandinavia and Northern Europe
and consisting mainly ofcoccoliths- the art historical aspectof coccolith study has been very fruitful here. Archaeological examples come from southern areas.
The following examples will be reviewed. They give an
incomplete but interesting overview of the work

ss==========================

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

accomplished during the past quarter of a century:
Ancient Mortar from Turkey and Egypt
The problem: was the fine material between the buildingblocks really mortar, that means the result of a man-madechemical process?
The answer, based on nannofossil study: no in one
and yes in the other case.
Mummy Cases from Egypt
The problem: none, really-sheercuriosity.
The answer: calcareous nannofossils found in the
ground of the paint include a Paleogene assemblage that
could have derived from nearby sources.
Icons from the former Soviet Union
The problem: none, really-sheercuriosity.
The answer: various ground of late Cretaceous age
was used. No attempt was so far made to investigate thepossible origin of the material.
Medieval churthes in Jutland, Denmark
The problem: few medieval churches in Denmark arebuilt of rocks from the underground - most are built ofbrick or of erratic blocks transported to Denntark by theglaciers during the ice-ages. Nine churches in thenortheastern part of Djursland are different, in that they
consist mainly oflocallimestones. Where did the limestones
come from? What were the transport routes? Why werecertain types of limestone used for construction and others
not?
The answer: Coccolith investigations by Erik Thomsen
using the Danian zones ofPerch-Nielsen ( 1979) allowed forthe detailed dating of the outcrops in the region and of thebuilding stones and therewith allowed for the determinationof the origin of the building blocks.
Ribe Domkirke, Denmark
The problem: Limestone used for the capital ofRibe
Domkirke (and for other sculptures) looked similar to local
danish limestone, but looked enough different to besubmitted to the author for investigation.
The answer: The coccolith assemblage includes anupper Cretaceous assemblage with not uncommon
Nannoconus . Such assemblages are not found in
Scandinavia, the limestone thus must have been imported.
Relief from Roskilde Domkirke, Denmark
The problem: A relief owned by the National Museumof Copenhagen was known to stem from the dome of
Roskilde. A wooden sculpture "head of Christ" from thedome ofRoskilde's "Triumfkrucifiks" was shown to havebeen painted over. Did the two pieces ofart originally belong
together and were part of the early french gothic aspect of
this church? Were they made in France or inDenntark?
The answer: Only the relief furnished coccoliths. Their
Maastrichtian aspect points to a local origin of the painting
ground and thus the object, rather than to an import from
France.
Other medieval Churches in Scandinavia andnorthern Europe
In medieval Norway and other Scandinavian and northeuropean countries, chalk ground was used to level andsmooth the surface of wooden sculptures and panels before
painting. The special interest of studying medieval chalkgrounds from Norway was based on the fact that here
exceptionally many medieval paintings are preserved andJournal of Nannoplankton Research, 17, 2, 1995.

that white chalk is not available in Norway itself. This led
to several questions:·where had the chalk come from?
· was the same source of chalk used everywhere in
Norway?
·was the same source of chalk used through the timefrom 1100-1550?
· does there exist any link between chalk provenanceand style?
To answer these questions, the distribution of chalk in
an area where it reasonably could have come from had to
be investigated. The distribution of chalk is quite wellknown in general. Less well known is, however, thedistribution of the various coccolith zones in outcrops or
quarries that might have existed at the time and that wereof easy access to sea transport.
Over 100 tiny samples from art objects from churches
were analyzed in the 1970-1980ies and their zonal
assignment determined mainly according to Sissingh ( 1977).
First results were published by Perch-Nielsen ( 1972) and in
Plahter et al. (1974 ). Further investigations answering theabove questions were presented in von Salis and Plahter(in press, 1995) and are summarised below.
The chalk used has come from different sources. During
the 12th and the early 13th century, chalk of late
Maastrichtian age (including Nephrolithus frequens) wasused widely in the north and east ofNorway. This is possibly
linked to the stylistic impulses received from southern
Scandinavia and northern Germany during that time. In
the western bishoprics, exclusively older chalk was used,
the origin of which most likely was southern England or
the Channel region. The chalk trade seems to have changed
around 1250, when the latter type of chalk was used allover Norway at the same time as an increase in influence ofEnglish style can be found in the whole of Norway. Latemedieval objects increasingly include the young chalk, afeature that conforms with the increased influence from
northern, now hanseatic Germany.
Besides objects from Norway, also chalk-grounds fromancient works of art from the Fcere Islands, Iceland,
Sweden, Belgium and England were investigated andpresented in von Salis andPlahter (in press, 1995). Whilethe "virgin" (period 1250-1400) fromKyrlgebi/J on theFcerr/J
Islands included an upper Maastrichtian ground possibly
deriving from Denntark, chalk ground from Morivellir on
Iceland from the period of 1250-1350 contained a Turonian
coccolith assemblage and thus chalk from England or the
Channel region. A 12th century crucifix from Hemse, Sweden
included a Santonian coccolith assemblage, while the sample
from St Halvard from Skresvikfumished a late Maastrichtianage.
The Belgian works of art dating from the 13th throughthe 17th centmy and including a Rubens and two Vermeer
paintings all contained chcillc of Santonian to Campanianage. These findings are partly supported by those ofRobaszynski (1988) who describes the presence ofSantonian white chalk from a medieval cave below the"Ancienne Maison De Greef'.
Svabeniclai (1993) reported Maastrichtian na:nnOfossils
from High Gothic paintings in Bohemia.

89========================~

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

REFERENCES
Perch-Nielsen, K. 1972. Fossil coccoliths as indicators of
Late Cretaceous chalk used in medieval art.
Universitetets Oldsaksamling. Lrbok 1970-71: 161-169.
Perch-Nielsen, K. 1979
Plahter, L.E., Skaug, E. and Plahter, U. 1974. Gothic painted
altar frontals from the church of Tingelstad. Material,
technique, restoration. Oslo.
Robaszynski, F.,1988. Nature et provenance de la craie
accumulee vers le XVe sii!cle sous I' Ancienne Maison
De Greef. Le Folklore Braban~n, 257:22-29.

Sissingh, W. 1977. Biostratigraphy of cretaceous
nannoplankton. Geol. en Mijnbouw: 37-65.
SvabenickA L. 1993. Maastrichtian nannofossils in thematerial of the High Gothic paintings in Bohemia. INA
Newsletter 15/2:96-97.
Thomsen, E. 19 · ·. Bygningsstenen i Grenaegnens
kalkstenskirker. · · ·von Salis Perch-Nielsen, K. and Plahter, U. in press/1995.
Analyses of fossil coccoliths in chalk grounds ofmedieval art in Norway.

NANNO NOTES: AN INTERACTIVE DIGITAL IMAGE CATALOG
OF CENOZOIC CALCAREOUS NANNOFOSSILS
Sherwood W Wise, Jr., Linda Tway, Darren D. Milman, Wi//iam C. Payton, James J. Pospicha/, Jay Muza,
Patrizia Maiorano, Andrea Concheyro, Giuliana Villa, Katharina Perch-Nielsen, Laurel M Bybe/1,
Jean M Self-Trail, Wil/iam L. Murphy, Wi//iam R. Riede/, and Yan Xu
Poster session
Nanno Notes is an icon-driven digital image catalog
consisting of over 600 illustrated calcareous nannofossil
taxa with original descriptions. The present version of thecatalog was developed for the Ocean Drilling Program toassist their micropaleontologists at sea where hard-copy
literature resources are limited. The program would also be
useful for students, teachers, and experienced professionals
making or refining taxonomic identifications at the
microscope. The program is written for the Windows
operating environment and, at this writing, has beendelivered to ODP for beta- testing aboard the JOIDESRESOLUTION.
When the program is opened, the first or "main" icon
screen presents the investigator with icons for 20 families,

closely related family groups and the catch-all "Incertae
sedes". Clicking on an ieon with the right button of themouse brings up a short text definition of the group, whereas
clicking the left mouse button brings up a second icon
screen that displays the genera within the selected group.
From this second screen generic definitions can be called
up as before with the right button of the mouse; the left
button, however, brings up a scroll list of species within
the genus. Clicking on a species name in turn brings up atext description and a set of illustrations of the taxon.
illustrations for up to 4 similar species can also be called up
and compared simultaneously on the computer screen.

THE INITIATION OF NORTH ATLANTIC DEEP WATER AS DATEDBY NANNOFOSSILS
Wuchang Wei
Monday, 14.00
The relatively warm, salty North Atlantic surface water
flowS into the Norwegian-Greenland Sea, releases heat andbecomes cold. The resulting denser water sinks and spills
over the sill between Greenland and Iceland (Denmark
Strait) and between Iceland and Scotland. This is North
Atlantic Deep Water (NADW), which follows contours
through the western Atlantic, moves southward andultimately spreads into the South Atlantic, Indian Ocean,and Pacific Ocean. NADW plays a vital role in theventilation of the world's deep oceans, distribution ofnutrient contents of deep water, and redistribution ofplanetary heat budget. Variations in NADW have been
considered to be an important factor controlling glacialinterglacial changes in atmospheric C0 2 • It is thus
fundamental to understand the history ofNADW. A basic
question of when NADW was initiated still remains largely
unanswered. A number of studies (e.g., Schnitker, 1980;
Blanc et al., 1980; Woodruff and Savin, 1989) proposedthat NADW began in the middle Miocene (13-15 Ma);
Miller and Fairbanks (1985) suggested that NADW existed

as early as the Oligocene; Wright et a!- (1992) argued that
NADW was produced from 20 to 16 Ma, and again from
12.5 Ma to the present. All these studies were based onrelatively indirect evidence (mostly carbon isotope data)from mid to low latitudes.
Here I use more direct evidence from ODP Hole 642B in
the Norwegian Sea and Hole 918D just south of theDenmark Strait to constrain the initiation ofNADW. Theinterval from the middle ofCore 642B-19 down to the bottomof the hole (early Miocene) is virtually non calcareous andthe benthic foraminifers are very rare and almost exclusively
agglutinated assemblages. NADW was apparently absent
during this time, when the Norwegian Sea water was
stagnant and bottom water was corrosive to carbonate.
The interval above the middle of Core 19 is calcareous,with abundant nannofossils, planktonic and benthic
foraminifers. This indicates the presence ofNADW, which
ventilates the Norwegian Sea and enhances the production
and preservation of calcareous planktonic and benthic
organisms. Core 19 is above the last occurrences of.

90========================~

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Cyclicargo/ithus jloridanus and Calcidiscus premacintyrei (both 12 Ma) and below the last occurrence of
Cocco/ithus miopelagicus (11 Ma). The initiation of
NADW is thus dated at about 11.5 Ma.
Core 38 ofHole 918D south ofthe Denmark Strait
contains glauconitic hardgrounds and glaucony rip-up
clasts. Benthic foraminiferal assemblages with Norwegian
Sea affinity begin to occur above this core. This suggests

Journal of Nannoplankton Research, 17, 2, 1995.

that Norwegian-Greenland Sea deep water began tooverflow the Denmark Strait sill at this time. This level isalso above the last occurrences of C. jloridanus and C.
premacintyrei and below the last occurrence of C.
miopelagicus.- This also suggests that NADW began. atabout 11.5 Ma.
Various sources of data from other areas are also reviewed and shown to be consistent with my interpretation
here.

CALCAREOUS DINOFLAGELLATE CYSTS AT THE KJT BOUNDARY OF THE
GEULHEMMERBERG (LIMBURG, THE NETHERLANDS)
He/mut Wi//ems
Wednesday, 9.40
The association of calcareous dinocysts is described forthe first time from the KIT boundary at the
Geulhemrnerberg (South Limburg, The Netherlands). A highdiversity of 31 morphotypes has been found, and 2
additional morphologically related incertae sedis organismsof the genus Bonetocardie//a. The dinocysts can be related
to the three subfamilies of calcdinocysts belonging to thefamily Calciodinellaceae DEFLANDRE 1947 within the
Peridiniinae: the Orthopithonelloideae with an orthogonal(radial), the Obliquipithonelloideae with an irregularly
oblique, and the Pithonelloideae with an uniquely obliqueorientation of the crystallographic c-axis of the calcite
crystals relative to the cyst surface.
The placement of the KIT boundary based on thevertical distribution of the calcdinocysts has to be takenwith caution as there is no clear evidence how much of thematerial has been reworked from the Campanian and
Maastrichtian. In the uppermost Maastrichtian as well as in
the lowermost Danian, the quantitatively dominating
representatives are the Pithonelloideae, nearly exclusively
Pithone//a sphaerica, accompanied by up to 14 %Bonetocardiella spp. Thus, both forms cross the KIT
boundary, which is new for the latter form. Whereas in the
Maastrichtian, Pithonella and Bonetocardiel/a occur
exclusively, Obliquipithonelloideae and Orthopithonelloideae occur with higher diversities in the lowermost
Danian. Most dinocysts in the Danian (22 of the 31 species)
are survivors of the boundary event, and only 8 species
first appear above the KIT.
The diversities of the Obliquipithonelloideae andOrthopithonelloideae show a variable distribution closely
connected to changing lithofacies. With up to 18 species,
the diversity is highest in the clay layers, especially in Clays
A, B, C, and E. In these horizons, the number oforthopithonelloid dinocysts increases in comparison to theobliquipithonelloid ones. In general, the lowest diversity isobserved within the calcarenites, and in some horizons thiscorrelates with the lowest frequency of specimens. The
cyclic diversity distribution of calcdinocyst morphotypes
may possibly be attributed to sea-level changes, whereas
the maximum transgression correlates to the diversity as
found in clay layers A/B, C, and E.

LIVING COCCOLITHOPHORID ASSEMBLAGES OFF THE
PUERTO RICAN SHELF
A. Winter and R. W Jordan
Monday, 9.40
In recent years, living coccolithophorids have received agreat deal of attention, mainly through the activities of the
Emiliania huxleyi programmes. However, since thecontributions ofOkada and colleagues in the 1970's, little
has been added to our knowledge of the composition ofassemblages and of the spatial and temporal distributionsof these organisms. This paucity of new information has
been influenced by a number of factors; a decrease in thefunding of floristic studies, a dwindling of taxonmnic
expertise, and the ever-increasing cost of running oceangoing research vessels. In addition, many scientific cruises
are of a short duration and contain a multidisciplinary teamof researchers, resulting inevitably in a compromised
sampling strategy. This state of affairs has led manyphytoplankton workers to become opportunistic samplers.

=========================91

At La Parguera (Puerto Rico), the University of Puerto
Rico has marine research facilities, including a small boat
capable of collecting oceanographic data. Over the last
three years, water samples have been taken at intervals of
two to three weeks from a number of depths (between 0140 m) at a station (1000 m water depth) located off theisland shelf. The aims of this project are 1) to study theseasonality and annual variation within the phytoplankton
community at a single station, 2) to assess the contribution
made by the coccolithophorids and to characterise their
species assemblage(s), 3) to determine the effect on thecommunity ofthe northward migration of the Orinoco Riveroutflow, and 4) to combine this floral data with theoceanographic information collected in-situ, in order toevaluate the possible ecological preferences of individual
species/assemblages.

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Coilference, Copenhagen 1995, Programme and Abstracts.

The samples have been filtered and are now being
analyzed. Preliminary observations of the filtered samples
suggest that diatoms and coccolithophorids compete forthe shelf space throughout most of the year. This reflects
the · dynamic physical and oceanographic setting of the
shelf environment. Within the coccolithophoridcommunity, Gephyrocapsa oceanica has been especiallyabundant in October when the Orinoco River outflow

migrates northwards, whilstEmiliania huxleyi and species
characteristic of subtropical gyres are common from March
to August. However, occasionally coccolithophorids are
entirely absent from shelf waters and diatoms predominate.
On one occasion calcite precipitating bacteria were themajor component at the station. Our studies indicate thatthe shelf and slope of Puerto Rico are much more dynamic
than previously thought.

NON- CONVENTIONAL NANNOPLANKTON BIOSTRATIGRAPHY APPLIED
TO BIOSTEERING HORIZONTAL WELLSCharles R. Young
Wednesday, 14.50
Non-conventional biostratigraphic techniques weresuccessfully used in steering and maintaining two
horizontally drilled North Sea wells (2/4 A-2la, 2/4 A-2a)
in a restricted target zone (upper third of the reservoir unit).
The techniques were initially applied to the 2n-I4x (wellnearest site of first horizontal well). Verification of thesetechniques in both the 2/4 A-2la (first horizontal well), andthe 2/4 A-8 (well nearest site of second horizontal well)eliminated the need for drilling, coring, and logging a pilot
hole in the 2/4 A-2a.
These techniques, which provide high resolution
nannoplankton zones with finet resolution than theconventional NN-NP or CN-CP zones, were used to
subdivide the major Tertiary reservoir unit (reworked
Cretaceous Zone, Field LayerED) of the Ekofisk Field into
three units. These techniques include: (a.) population
dynantics, (b.) polar ordination, (c.) morphornetric analyses,and (d.) synchronous variation of nannofossil assemblages
and petrophysical parameters.
a) The middle unit of the reworked Cretaceous zone
was defined by a marked increase in the abundance ofLucianorhabdus cayeuxii plus the influx of reworked
Campanian taxa.

b) Polar ordination of the nannoplankton assemblages
through layer ED verified the three subzones, plus thepossibility of a fourth.
c) Morphometric measurements of the reworked
Cretaceous taxa Arkhangelskiel/a cymbiformis reflected
the same three subdivisions.
d) Two "spikes" in Thoracosphere-Ca/cisphereabundance, which can be used as a proxy for silica
abundance, flag two porosity-permeability partitions in thereservoir. These partitions occur at, or near, the subzone
boundaries.
The technology, techniques and zonal scheme, wastransferred to the Stavanger office and was subsequently
used, on wellsite, by paleontologic consultants during thedrilling ofboth horizontal wells.
I would like to acknowledge Phillips Petroleum
Company Norway and eo-venturers, including Fina
Exploration Norway S. CA, NorskAgip AIS, ElfPetroleum
Norge a.s., Den Norske Stats Oljeselskap as., 1DTAL Norge
AS.,ElfRexNorgeA/S,andNorminolA/Sfortheirfinancial
support and permission to publish this paper. The opinions
expressed are those of the author and do not necessarily
represent those of Phillips Petroleum Company and eoventurers.

COCCOBIOM - A LIGHT MICROSCOPE BASED IMAGE CAPTURE AND
MORPHOMETRICS APPLICATION FOR EMILIANIA HUXLEYIAND OTHER COCCOLITHS
Jeremy R. Young, Jackie A. Burnett, and Michal Kucera
Monday, 15.15
In order to produce quantitative data on key aspects of themorphology of Emi/iania huxleyi coccoliths an automatedimage analysis system has been developed (Young et al. inpress). The system is based on an Apple Macintosh
microcomputer with .direct image capture from a Zeiss
Axioplan Photomicroscope via Sony XC77 8-bit CCD andPerceptics Framegrabber. Cross polarised light images areused. The software used is NIH-Image, developed by W,
Rasband of the National Institutes of Health. Within thispackage the macro programming language has been used
to develop a coccoliths biometrics application. The
application consists of two parts, image capture routinesand biometrics routines.

For the image capture routines the user identifies
coccoliths on the live image by placing the cursor within
their central area. The coccolith image is then copied into acomposite mosaic image. The final mosaic images consistof60 separate coccolith sub-images in a regular array.
The biometric routines commence with identificationof the most distinctive feature of the coccolith images, thefour maximum brightness peaks. These are used to determine
the geometric centre of the coccolith. Using this centre, an
ellipse fit is then performed on the four peaks plus some
additional points on the central area edge. This gives theorientation, length and width of the central area ellipse.
The outer edge of the coccolith is then located at four

92========================~

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995.

A. IMAGE ACQUISITION
Screen grao Showw"uJINt •maoe. Clrect trom tr~~Croscooe ana mc:..IC •m~ us.a lOt soeeunen stor• . Specunens art stttC1ed Wll'tltne
cursot '" tnt l•ve .mage and transtetrec:lto lnt mosa.c magea s~e moute elrcK . Crtallng a rnoaa•c tmage o1 60 speamens taka
10-15 mmutts

••th

, "'

.. . 00.::N-,oJ~:~

4:-tl 00~':'tOO~,

00' '!'9,.,:~500.' ':'1~....
""' ,,'",,,""' ,,.,. ... ..
, .. ., ..
,..,,.,
, 00
,. 00

lOO

-JI U

,

-14 . ,

]

,00

n

ll
•• &l

•oo ,.

"00)

101 . ,

'"
'

"

'

lO

- ~· 00' ) 01

; 72

·6 )4

'

000
0 .,
0 ••

~

•-Jt '50..... ..,
.. 0"

'"

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"
'

' "'

'

...
,.,.

: 01

066

' •o

0 ':' 4

;: 01

~~

'

7"('

J•ll

j

ll. IMAGE ANAL YSISIMORPHOMETRICS
S.:reero qrao snow.nq mos~c . auer IDK•mens h.lvt oe.o measureo .Jt• CJ tne reosunanc aara hit The measurement procen '' ent•retv automateo .ind takes.100ut 2 m1nu1es per mosa•c A manual aata '<~tnhcat•on step'' "'en ,..,f'O~ T,.eo sunace o+ot •• a repre 5.,u1t•on ot ongntness over one soec•m~ t•tCI '"me mosa•c •maQe . •I snows !nf' ouetnnqence pea .. s wruch are a"I!'" ·••1\olre ... s.o on tne trf\i198 an~y115

Fl~:ure: Coccobiom Morphometric system. The system to be used for producing quantitative data on Emiliania huxleyi morphometricvariation. This is based on capture of cross-polarized light microscope images to a Macintosh computer using the program NIH-Image anda custom set of macros.

After this automated phase the user reviews the displayed
results and additional macros allow rapid manual correctionof suspect results. This is rarely needed for the central area
measurements but is often needed for the rim width
determination.

points on radial transects outward from the maximum
brightness peaks and the rim width is calculated from thesepoints. The measured results are stored and displayed
graphically on the image. This process is entirely automaticand is repeated on each specimen of the mosaic image.

93

Journal ofNannoplanlcton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

The maximum resolution of the results is detennined by
the pixel width (0.06 )..l.m). Control experiments involving
repeat measurements of individual coccoliths suggest an
accuracy of about +/-{) .1 1J.II1 for the central area parametersand +/-0.2 J..l.m for the coccolith length (calculated from
centrnl area length+ 2 x rim width).
Although the system has been specifically developed
for work with Emi/iania huxleyi it has considerable
potenrtial for being applied to other coccoliths. The
automated biometric routines would need rewriting for
application to other coccoliths but the semi-automatedroutines are of much wider application. The mosaic creation
routines are of universal applicability for nannofossil workand provide a very convenient means of rapidly collecting
light microscope images.
This work was funded by the EC-MAST as part of"Cocco1ithophorid dynamics: the European Emi/iania
huxleyi programme (EHUX)".

REFERENCE

Young J .R ., M. Kucera, Hsiao-Wen Chung , (inpress). Automated coccolith biometrics on captured lightmicroscope images of Emiliania huxleyi. For,
Proceedings of the ODP and the Marine Biosphere
Conference, Aberystwyth, April 1994.

STUDIES OF COCCOLimOPHORIDS FROM THE ARABIAN SEA
AND THE NORTH INDIAN OCEAN
A/exandra Ze/tner
Poster session
The assemblage composition and the distribution patternof living coccolithophorids in the upper photic zone (20 m)of the Arabian Sea is described. Sampling was carried out
duringMarchandMay 1995, R V. METEOR-cruiseM3113
and M32f3 . Employing Wclter samplers, 229 nannoplankton
samples were taken off the Arabian Sea and the North Indian
Ocean between 20 and 2500 m water depth. While sampling
the atmospheric and oceanic circulation was impressed by
the northeastern monsoon (March) and by theintermonsoonal period (May). Scanning Electron
Microscopy (SEM) was utilized for the taxonomical
identification and to quantify the standing crop of
coccolithophorids. At minimum 300 coccospheres werecounted on transects at a magnification of 4500_ (eachfield measured 374 _m 2). More than 30 heterococcolithophore and six holococcolithophore species wererecorded in samples collected March 1995, during
northeastern monsoon. The floral assemblage during thattime is dominated by Emiliania huxleyi (Lohmann) Hay
and Mohler and Gephyrocapsa oceanica Kamptner. The
cooccurrence of Emiliania huxleyi and Gephyrocapsa
oceanica indicates a nutrient-enrichment in upwelling areas(Kleijne 1993 ). Very significant for the hydrography is the
low abundance of holoeoccolithophorids in the samples.
This situation changes in the inteimonsoonal period. The

species diversity seems to be much lower. In theintermonsoonal period eight heterococcolithophore,
dominated by Umbellosphaera irregularis Paasche andU. tenuis (Kamptner), and an increased number ofholococcolithophore species, which prefer a low nutrient
concentration, occur. This species composition reflects
oligotrophic conditions.
Although the assemblage of holococcolithophores
during May is completely different from theholococcolithophore community during the northeastern
monsoon, some heterococcolithophore species likeEmi/iania huxleyi, Gephyrocapsa oceanica,
Discosphaera tubifera, and Coronosphaera
mediterranea., Umbel/osphaera irregularis, and U tenuis
are recorded in the samples of both cruises. These species
show a wide range of physico-chemical tolerance.
This distinct temporal distribution reflects the seasonalchange of oceanic currents as a result of monsoon.

REFERENCE

Kleijne, A., 1993. Morphology, taxonomy and distribution ofextant coccolithophorids (calcareous nannoplankton) I
Annelies Kleijne.-[S.l. : s.n.] (Enschede : FEBO). - Ill.
Proefschrift Vrije Universiteit Amsterdam. - Met. lit. opg. Met samenvatting in het Nederlands.

94===========================

Journal of Nannoplankton Research, 17, 2, 1995 .

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

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6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplanlcton Research, 17, 2, 1995.

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Journal of Nannoplankton Research, 17, 2, 199~.

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6th INA Conference, Copenhagen 1995, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995 .

PROGRAMME
2nd - 7th September 1995
Monday, 4 September

8.30-9.15

REGISlRATION

9.15-9.40

IN1RODUCTIONANDWELCOME

9.~10.05

A. Winter and R. W. Jordan : Living coccolithophorid assemblages off the Puerto Rican
shelf

10.05-10.20

1EA-COFFEEBREAK

10.20-10.45

Dorothea Janofske, Helmut Keupp and Helmut Willems : Calcareous dinoflagellate cysts:
ultrastructure types and systematic application

10.45-11.10

Harald Andruleit : Production, Sedimentation and Preservation of Coccolithophores in thenorthern North Atlantic

11.10-11.35

Mario Cachi\o and M. T. Moita : Cocco/ithus pe/agicus, a sort of productivity proxy?

11.35-12.00

Llu'i sa Cros : Coccolithophorid distribution across a transect between the Iberian Peninsula andthe Balearic Islands (northwestern Mediterranean Sea)

12.00-12.25

Alex Chepstow-Lusty and Mark Chap man : An examination of the global relationship between
the last two "species" ofDiscoasters at the end of the Pliocene.

12.25-12.50

Xin Su : Development of the Plio-Pleistocene coccolith assemblages in the NE Atlantic correlated
to climatic changes

12.50-14.00

LUNCH

14.00-14.25

Wuchang Wei : The initiation of North Atlantic deep water as dated by nannofossils

14.25-14.50

Beate Kerntopf : Calcareous dinoflagellates of the equatorial Atlantic Ocean

14.50-15.15

Beige Thomsen : Polar coccolithoporids

15.15-15.40

Jeremy R. Young, Jackie A. Burnett, and Michal Kucera: Coccobiom- a light microscope
based image capture and morphometries application for Emiliania huxley! and other coccoliths.

15.40-16.00

lEA-COFFEEBREAK

16.00-16.25

Patras Dimitris Frydas : Biostratigraphy using silicoflagellates and calcareous nannofossils of
Neogene-Pleistocene deposits of Greece

16.25-16.50

Priscilla J. Militante-Matias and Marietta M. de Leon : A study of the forarniniferal andcalcareous nannoplankton assemblages of core samples taken from the Lahar-affected portionsof the South China Sea in Zambales Province, Philippines

16.50-17.15

Jacques Giraudeau and Geofl'rey W. Bailey : Sediment trap studies of coccolith and planktonic
foraminiferal fluxes in the Benguela upwelling system

Tuesday, 5 September

9.15-9.40

Koji Kameo, Tokiyuki Sato, and Toshiaki Takayarna : Late Pliocene nannofossil bioeventsand their biostratigraphic and paleoceanographic meanings
Nicolae Meszaros : Nannoplankton in the volcanic tuffs of the Transylvanian Basin (Miocene)

10.05-10.20

lEA-COFFEEBREAK

10.20-10.45

GROUP PHOTO

10.45-11.10

Viviane Reale : Paleoecology of calcareous nannofossil assemblages and its relationship to sealevel variations in the Figols Group (Early Eocene, Spanish Pyrenees)·

11.10-11.35

Eric de Kaenel : Paleocene to Early Eocene calcareous nannofossil biostratigraphy based on the

EL-Kef section (Tunisia)===========================98

Journal of Nannoplankton Research. 17, 2, 199S.

6th INA Conference, Copenhagen l99S, Programme and Abstracts.

11.35-12.00

James J. Pospichal : Calcareous nannoplankton, Tsunarnites, and the Kif boundary ofnortheastern Mexico

12.~12 . 25

Akmal M. Marzouk and Mohamed K. Abou-EI-Enein : Calcareous nannofossil biostratigraphyof the Late Cretaceous-Early Tertiary of Wadi Feiran and Gebel Qabeliat, south western Sinai,Egypt

12.25-12.50

Yoram Eshet and AhuvaAimogi-Labin : Calcareous nannofossils as paleoproductivity indicators
in Carnpanian-Maastrichtian upwelling systems

12.50-14.00

UJN<ll14.00-14.25

Jim A. Bergen : Cenomanian nannoplanklon minor extinctions in low to mid-latitude shelfsections: calibration to ammonite and sequence stratigraphy (abstract missing)

14.25-15.40

POSTER SESSION

15.40-16.00

1EA-COFFEEBREAK

16.00-17.40

POSTER SESSION

Wednesday, 6 September
9.15-9.40

Jean Self-Trail :Late Cretaceous biostratigraphy and paleoceanography of the Atlantic Coastal
Plains, USA

9.40-10.05

H. Willems : Calcareous Dinoflagellate Cysts at the Kif Boundary of the Geulhemmerberg(Limburg, The Netherlands)

10.05-10.20

1EA-COFFEEBREAK

10.20-10.45

F. Naji: Calcareous nannoplankton biostratigraphy of the Salzgitter-Salder Limestone Quarry,
Lo~rSaxony,Germany

10.45-11.10

Jorg Mutterlose : Calcareous nannofossil paleoceanography of the Lo~r Cretaceous of northwest
Europe11.10-11.35

Andrea Fiorentino : Maastrichtian nannofossil biogeography in the Southern Tethys

11.35-12.00

Francesca Lozar : Calcareous nannoplankton biostratigraphic analysis as a tool for the study of
discontinuity surfaces in the Cretaceous of the Trento Plateau (southern Alpine, Italy)

12.~12.25

Marie-Christine Janin, Yann Samson, Maria Saint-Gennls, Fran~ois Baudin and Gerard
Bignot : Comparative variation of calcareous nannofossils (especially Ellipsagelosphaeraceae),
foraminifers and organic matter concentration in the Kimmeridgian sequence from la Briere(Normandy, France)

12.25-12.50

P.R. Down and C. Ellison : Jurassic-Early Cretaceous calcareous nannofossils from the Neuquen
Basin, Argentina

12.50-14.00

UJN<ll14.00-14.25

Katharina von Salis : Calcareous nannofossils in the arts .

14.25-14.50

Magdy H. Girgis : High resolution nannoplanklon biostratigraphy and steering horizontal wells(abstract missing)

14.50-15.15

Charles R. Young : Non-Conventional Nannoplankton Biostratigraphy Applied to Biosteering
Horizontal Wells

15.15-15.40

Martin Jakubowski : Biostratigraphy in the oil industry

15.40-16.00

1EA-COFFEEBREAK

16.00-16.25

David Jutson : The Case of the Missing Nannofossil or "Now you see it, now you don't".

16.25-16.35

FAREWELLADDRESS

18.30

CONFERENCE DINNER

Srllpavillonen, Gyldenlrllvegade 24, Copenhagen K.

=======================99=======================

6th INA Conference, Copenhagen 199S, Programme and Abstracts.

Journal of Nannoplankton Research, 17, 2, 1995.

POSTERS
J. Alcober and R. W. Jordan : Neosphaera coccolithomorpha and Ceratolithus crista/us: are they the same species?
Filomena Ornella Am ore : Calcareous nannofossils from Calvello Basin (southern Apennines, Italy)
Gregor Bischoff and Jlirg Mutterlose : The turnover of calcareous phytoplankton from the Barrernian-Aptian boundaiy
interval in NW Europe
P.R. Bown, S. Davies, J. Didymus, T. W. Ehrendorfer, S. Mann and J.R. Young : Coccolith building blocks: highresolution analyses ofHeterococcolith morphology and crystallography
Jackie Burnett : Albian/Cenornanian to Kif Stage boundaries and nannofossil events: increased precision in Upper
Cretaceous nannofossil biostratigraphy and correlation
Georges Busson, Denise Null, F~oise Monniot and Annie Cornee : Some calcareous nannofossils misinterpreted inliterature as Tetralithus, Triquetrorhabdulus, Fusellinus sp. Are actually spicules of Didemnum ssp. (Tunicata,
Ascidian). Evidence from Upper Jurassic sediments of Charentes (W. France)
A. d' Atri, A. Novaretti, R. RufTmi, M.A. Cosca and J.C. Hunziker : Calcareous plankton biostratigraphy and 40Arf39 Ar
dating of volcanic ash layers from Monferrato (NW Italy) (abstract missing)
Agata Di Stefano : Calcareous nannofossils biostratigraphy of the Plio-Pleistocene deposists of the Peloritani Mountains(NE Sicily)
Y. Eshet, T. Minster, S. Moshkovitz : Calcareous nannofossil datum levels: a key for the understanding of the genesis ofUpper Cretaceous oil shale sections in Israel Carnpanian-Maastrichtian Oil Shale
Y. Eshet and S. Moshkovitz : Calcareous nannofossil biostratigraphy in Santonian-Maastrichtian organic-rich carbonate
sections in Israel
Claire Findlay : Calcareous nannoplankton from the Australian Sector of the Southern Ocean
J.A. Flores, F.J. Sierro, L Zamarreno, A. Vazquez, R. Utrilla and G. Frances : An Example ofEutrophic..Qligotrophic
alternances in the Lower Messinian: The Sorbas Basin (Western Mediterranean)
Silvia Gardin and Nicola Perilli : Early Cretaceous calcareous nannofossil biostratigraphy of the internal Ligurids(northern Apennines, Italy) and the onset of coccolith-bearing sediments in the Ligurian-Piedrnont oceanic
domain
WiUiam W. Hay : Oceanic fronts in the Mesozoic
Tania Hildebrand-Habel and Helmut WiUems : Calcdinocysts from the middle Coniacian to upper Santonian chalks at
Laegerdorf (N Germany)
Ramses P. Hoek and Karin A. F. Zonneveld : Upwelling related dinoflagellate cyst associations of the Benguela current
system.
Christine Hoell : Correlation of calcareous and organic-walled dinoflagellate cyst associations in glacial/interglacial
cycles, an example of the Equatorial Atlantic
Glen Homeier : Mid-Cretaceous calcareous nannoplankton in an organic-rich facies of the Subbetic and Penibetic (Betic
Cordillera, southern Spain)
Richard Howe : Mid-Late Cretaceous nannofossil biostratigraphy of the Papuan Basin, Papua, New Guinea
Dorothea Janofske, Helmut Keupp and Helmut WiUems : Calcareous dinoflagellate cysts: ultrastructure types andsystematic application
Helmut Keupp : Calcareous dinoflagellate cysts of the Late Albian and their environmental deductions (borehole Kirchrode
191, Gennany)
Ulrike Kienel : Development of calcareous dinoflagellate cysts (Calciodinellaceae Deflandre, 1947) at the CretaceousTertiary boundary (NE Germany, Denmark)U. Kienel, U. Rehfeld, S. BeUas and R. Kohring: The Miocene Blue Clay Formation of the Maltese Islands: Sequencestratigraphic and paleoceanographic implications based on calcareous nannofossil stratigraphy and calcareous
dinoflag(;Uat(; qsts.

===========================100===========================

Journal of Nannoplankton Research, 17, 2, 1995.

6th INA Conference, Copenhagen 1995, Programme and Abstracts.

H. Kinkel, N. Dittert, KH. Baumann : A 300 kyrs calcareous plankton record of the equatorial South Atlantic:
Reconstructions of surface water productivity and bottom water dissolution cycles
Anna Lototskaya and Patrizia Ziveri : Calcareous nannoplankton response to termination II and Heinrich event ( 140-110
KA BP) in the NE Atlantic
Patrizia Maiorano, Maria Marino and Simonetta Monecbi : Pleistocene calcareous nannofossil biostratigraphy of Site
577 Leg 86, Northwestern Pacific Ocean
Maria Marino : Calcareous nannofossil biostratigraphy of early-middle Pleistocene terrigenous sediments (Southern
Italy)
Emanuela Mattioli and Nicola Perilli : Calcareous nannofossils biostratigraphy of the Fuentelsaz (Spain) and Fiuminata(Italy) Sections: Late Toarcian-Early Aalenian
E. Mostajo,A. Concbeyro, F. D zquez: Calcareous Nannofossils (Hauterivian) from "Agua de laMula" Section, Neuquen
Province, Argentina.
Andras N agymarosy : The nannoplankton of the Jaslo Limestone horizons
Jemej Pav§i~ and Tadej Dolenec : Floristic and isotopic changes at the Paleocene-Eocene boundary in Slovenia
Alyssa Peleo-Alampay : Morphometric and Biochronologic Study ofCoccolithus miopelagicus
James J. Pospicbal : Calcareous nannofossils, Tsunamites and the Kif boundary of northeastern Mexico
M. Pramparo, W. Volkbeimer, and E. Mostajo : Calcareous nannofossils and palynomorphs from Valanginian andHauterivian (Lower Cretaceous) strata ofCerro de la Parva, central-western Neuquen, Argentina.
Anna Romaniv : Calcareous nannoplankton from the boundary deposits ofMaastrichtian and Danian of the Ukrainian
Carpathians
Antonieta Sancbez-Rios, Hector Ruiz-Ruiz, PatriciaPadilla-Avila, and J . Manuel Grajales-Nishimura: Nannofossils
and planktic forarninifera across the K!f boundary in two sections of northeastern Mexico
Tokiyuki Sato and Koji Kameo : Late Pliocene nannofossil events recognized in the uppermost sequence in the Japan
Sea side, with reference to the glaciation in the Arctic Sea
William G. Siesser : Paleogene and Neogene productivity in the Indian Ocean
Lilian Svabenick8 : Rare occurrences ofPelrarhabdus copu/atus Deflandre on the northern hemisphere (Central Europe)
Erik Tbomsen :The Danian (Lower Paleocene) limestone deposits in Denmark: basin development and sequencestratigraphy.
Maola Usbakova : Changes of calcareous nannoplankton evolutionary diversity during the Paleogene
S. Volin, Y. Esbet, and H. Kisb : Utility of calcareous nannofossils and organic remains: in the reconstruction of thermal
metamorphism in the Hatrurim Formation (Tertiaiy, southern Israel)

I
,-

r-

Sherwood W. Wise, Jr., Linda Tway, Darren D. Milman, William C. Payton,James J. Pospicbal, Jay Muza, Patrizia
Maiorano,Andrea Concheyro, Giuliana Villa, Katharina Perch-Nielsen, Laurel M. Bybell, Jean M. SelfTrail, William L. Murphy, William R. Riedel, and Y an Xu : Nanno Notes: An interactive digital image
catalog ofCenozoic Calcareous Nannofossils
Alexandra Zeltner : Studies of Coccolithophorids from the Arabian Sea and the North Indian C>cea1}=========================tot===========================