12th INA Conference, Lyon, 2008, abstracts © 2008 International Nannoplankton Association
ISSN 1210-8049 Printed by Cambridge University Press, UK

Lyon, 2008
12th INA conference, September 7-13th12

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http://www2.plymouth.ac.uk/science/cretaceous/Abstracts

9

The last 20kyr in the Alboran Sea from the coccolithophore
record: preliminary results
M. Carmen Álvarez, Lluïsa Cros, Belén Alonso, Javier Alcántara-Carrió
We are showing preliminary results from the gravity core
ALM6. It was recovered by the R/V “Garcia del Cid” ofthe ICM (Instituto de Ciencias del Mar, Barcelona) during
the expedition MAYC-96. The main purpose was to obtain
information about the coccolithophorid record of the last
20 ky.
ALM6 is located at the base of slope of the Almeria
margin (Alboran Sea, 36.35ºN, 2.61ºW) at a water depthof 1456 m. We studied 41 muddy hemipelagic samples obtained from a 5 cm systematic sampling. The age model
was obtained from the AMS-carbon 14 radiocarbon analyses on tests of Globigerina bulloides. The calendar ages
were obtained using the OxCal v3.10 (Bronk Ramsey,
1995; 2001) calibration program computer. Bottom core
was about 20 ky B.P. and the estimated sedimentation rate
was about 12 cm/ky. However, sedimentation rate washigher during Pleistocene than Holocene (Bozzano et al., inpress).
A filtering technique was combined to the technique described in Flores & Sierro (1997) to prepare coccolithophore samples in the laboratory. Observations weremade using a SEM (2000x) and counting around 300 coccoliths per sample (Fatela & Taborda, 2003).
The identification and counting of coccoliths revealed
that Emiliania huxleyi was the dominant species. Other
abundant taxa were: Gephyrocapsa spp., Syracosphaeraspp., Calciosolenia spp. and Umbilicosphaera spp.
The preservation degree was estimated as “good” (Flores et al., 2003). It has been possible to observe resistanttaxa (C. leptoporus) coexisting with other, more easily dissolved coccoliths (small placoliths) in the same sample.
References
Bozzano, G., Alonso, B., Ercilla, G., Estrada, F. & García, M.
Late Pleistocene and Holocene depositional facies of the
Almeria Turbidite System (Western Mediterranean). In: B.
Kneller, McCaffrey, O. Martinsen & H. Posamentier (Eds).
External Control on deep water depositional systems: Climate, seal-level and sediment flux. Geological Society of London (in press).
Bronk Ramsey, C. 1995. Radiocarbon calibration and analysis ofstratigraphy: The OxCal program. Radiocarbon, 37(2): 425430.
Bronk Ramsey, C. 2001. Development of the radiocarbon calibration program OxCal. Radiocarbon, 43(2A): 355-363.
Fatela, F. & Taborda, R. 2003. Confidence limits of species proportions in microfossil assemblages. Marine Micropaleontology, 45: 169-174.
Flores, J.A. & Sierro, F.J. 1997. Revised technique for calculation of calcareous nannofossil accumulation rates. Micropaleontology, 43: 321-324.
Flores, J.A., Marino, M., Sierro, F.J., Hodell, D.A. & Charles,
C.D. 2003. Calcareous plankton dissolution pattern and coccolithophore assemblages during the last 600 kyr at ODP Site

1089 (Cape Basin, South Atlantic): Paleoceanographic implications. Palaeogeography, Palaeoclimatology, Palaeoecology, 196: 409-426.

10Abstracts

Upper Cretaceous to Paleogene of the Dahomey Basin:
calcareous nannofossil biostratigraphy
Cleber Fernandes Alves, Eduardo Apostolos Machado Koutsoukos, Maria
Dolores Wanderley
The present work aims to identify and correlate the Maastrichtian to middle Eocene calcareous nannofossil assemblages of the southern Dahomey Basin. This is an extensive
sedimentary basin located in the Gulf of Guinea, spreading over the central West African margin from Ghana to
Togo and Benin to the west, and along southern Nigeria tothe east.
Five well-sections (cored well Ilaro-3, Ilaro-1, Araromi
and Wasimi, and well Bode Ashe, with ditch-cuttings), andone outcrop section (Shagamu) were selected to be studied. A detailed biostratigraphic framework based on calcareous nannofossils is proposed for the Maastrichtian tomiddle Eocene of this region.
The calcareous nannofossil study of the selected successions recovered the following bio-chronostratigraphic
intervals:
Bode Ashe well: Maastrichtian to middle Eocene, biozones
CC26, NP1-NP4, NP6-NP9, NP10, NP11/NP12 andNP13/NP14.
Ilaro-3 well: Eocene, biozones NP12, NP13, NP14 and
NP15.
Ilaro-1 well: lower Paleocene to middle Eocene, biozones
NP1, NP2-NP4, NP5/NP6, NP7/NP8, NP9 and NP10.
Araromi well: Maastrichtian to lower Eocene, biozones
CC26, NP1, NP4, NP5, NP6, NP7/NP8, NP9 and NP10.
Wasimi well: Maastrichtian, biozone CC26.
Shagamu outcrop: upper Paleocene, biozone NP9.
This was a joint project coordinated and carried out by
PETROBRAS-CENPES (Rio de Janeiro), the Technische
Universität of Berlin (TUB, Germany), and the University
of Ilorin (Nigeria). The financial support by the Volkswagen-Stiftung Program of Partnerships is gratefully acknowledged. The present calcareous nannofossil study wassponsored by a doctorate scholarship of the Program of
Qualification of Human Resources in Petroleum GeologyPRH-ANP/MCT 18/UFRJ.

Abstracts

11

Distinctive new deep-photic coccolithophore taxa from theJava upwelling system (eastern Indian Ocean)
Harald Andruleit
Extant coccolithophores have been intensively studied overthe past two decades and their taxonomy is probably better
established than that of any other phytoplankton group.
Nonetheless new taxa continue to be recorded, especiallyfrom the deep-photic zone and the number of very distinctive but rare coccolithophores is a curious feature of thisextreme habitat (Young & Andruleit, 2006).
Several of such unusual new coccolithophore species
were found during examination of samples from the eastern Indian Ocean off SW Indonesia under the influence of
the Java upwelling. In this monsoonal influenced area theoceanographic environment exhibits a high variability witha seasonal change from oligotrophic to eutrophic conditions. Today, upwelling seems to recur only for a short time
period around September, whereas oligotrophic conditions
prevail during most of the year. In the geological record,
however, upwelling-indicating species evidently dominate
the assemblages (Andruleit et al., in press).
Some of the new species described here are rather sim-

ilar to already known or recently described species. Other
species show remarkable new features and are not easily
related to already established genera or families. Although
the nature of some of the shown specimens is not clear,
their morphology, size and structure suggest an origin
within the coccolithophores.
A detailed description of the potentially new coccolithophore species will be published in detail elsewhere.
Here, selected specimens (Figures 1 to 9) are shown for
discussion within the scientific community.
References
Andruleit, H., Lückge, A., Wiedicke-Hombach, M. & Stäger, S.
Late Quaternary development of the Java upwelling system(eastern Indian Ocean) as revealed by coccolithophores. Marine Micropaleontology, in press.
Young, J.R. & Andruleit, H. 2006. Navilithus altivelum: a remarkable new genus and species of deep photic coccolithophores. Journal of Micropalaeontology, 25(2): 141-152.

12

Abstracts

Eastern Mediterranean Sapropel 1 (S1) dynamics from
coccolith chemistry
Lia Auliaherliaty, Patrizia Ziveri, Heather M. Stoll
The eastern Mediterranean Sea is an area where occasionally sapropel (organic-rich layer deposited under seafloor
anoxic conditions) formation took place. The occurrenceof these layers corresponds with the summer insolation
maxima of the Northern Hemisphere, which increases theseasonal thermal gradient between ocean and continental
regions and thus enhancing the African monsoonal circulation system. The driving mechanism of sapropel deposition is still debatable however, the combination of bothanoxia of the bottom-water and enhanced marine productivity, as a response to the climate forcing (Emeis et al.,2000) could explain it.
Coccolithophores are a dominant phytoplankton groupin the Mediterranean Sea and an important indicator of pastconditions in the fossil record. In the eastern Mediterranean, the significant increase of Florisphaera profunda
during S1 was correlated with a nutrient-rich lower photic
zone and stratification of the upper water-column.
To reconstruct the dynamics of S1 formation, we analyzed species-specific coccolith stable isotopes on fourdeep-sea sediment cores spanning S1 from the eastern
Mediterranean, and one from the western Mediterranean.
The oxygen isotopes of species-specific coccolith carbonate may infer the oxygen isotope composition of the seawater, which is affected by temperature, evaporation, andprecipitation. The δ13C of the dissolved inorganic carbon(DIC) in seawater is influenced by the production and respiration of organic matter. We also present results on Sr/Ca
ratios as a proxy of productivity from two cores.
The fine fraction (<20 μm) record showed a shift ofabout ~ 0.5 to 2 ‰ in δ18O and ~1 ‰ in δ13C. The fine fraction carbonate in the Mediterranean Sea is made up of not
only several coccolith species (vital effects in δ18O andδ13C) but possibly also reworked coccolith species andfragments of other unidentified biogenic carbonate. Emiliania huxleyi enriched fraction (3-5 μm) showed a negative shift of about ~ 1 ‰ in δ18O and δ13C. The δ18O results
combined with alkenone temperature reconstructions fromthe same samples confirmed a large freshwater discharge
before sapropel formation. An increase of freshwater input
will establish a low-salinity surface layer, thus modifying
the thermohaline circulation of the eastern Mediterranean
by weakening the Eastern Mediterranean Deep Water formation and promoting a termination of deep water ventilation. This condition might lead to the oxygen depleted zone
which caused accumulation and preservation of the organic-carbon-rich sediments. Furthermore, an increase ofcontinental influence may fertilize the basin and lead to relatively high productivity.
A parallel trend of negative shifts in the δ18O and δ13Cof both fractions mirrored the Sr/Ca ratios which showed
an increase of ~ 1.5 mmol/mol for fine fraction and ~ 0.75

mmol/mol for E. huxleyi enriched fraction. These results
clearly suggested an increase in productivity during S1 inthe eastern Mediterranean. Nevertheless, the record in thewestern basin showed no response to such climate change
during S1 time interval.
Reference
Emeis, K.C., Sakamoto, T., Wehausen, R. & Brumsack, H-J.
2000. The sapropel record of the eastern Mediterranean Sea results of Ocean Drilling Program Leg 160. Palaeogeography, Palaeoclimatology, Palaeoecology, 158: 371-395.

Abstracts

Highly variable Holocene climate from the Laurentian Fan
using coccolith and palynomorph proxies
Barbara Balestra, Adele Bertini, Anne de Vernal, Simonetta Monechi, Viviana
Reale
Coccolith, dinocyst and pollen analyses from the IMAGES
core MD95-2033, collected from the Laurentian Fan (lat:44˚39.87N, long: 55˚37.21W; water depth 1412m), provide
new data set in millennial scale, to assess the magnitude ofclimatic changes during the Holocene. Today, the area isunder the influence of the North Atlantic Current (NAC).
North Atlantic circulation, through its heat transport anddeepwater formation, is an important contributor in the climate system. Several dramatic reorganizations of the ocean
circulation have occurred during the last glacial and interglacial period. During the Holocene period in particular,
the surface ocean circulation shows different patterns andthe mechanisms behind them are very still much under debate.
In this research, coccolith, dinocyst and pollen diversity and concentrations are used as proxies to trace thosesurface water circulation changes. In particular, in the coccolith assemblages, the abundances of Emiliania huxleyi,
Calcidiscus leptoporus and Gephyrocapsa spp. show millennial-scale oscillations. Dinocyst assemblages are dominated by Operculodinium centrocarpum followed by
Spiniferites elongatus, Bitectatodinium tepikiense andAlexandrium excavatum. These species show large-amplitude temperature and salinity fluctuations, which indicate
major climate and/or hydrographic change, at least on a regional scale. Estimates of sea-surface temperatures, salinity and sea-ice cover, reconstructed using dinocysts, werealso performed.
This work provides new data in order to better understand the key processes in Holocene regional cooling andwarming of North Atlantic surface waters and the variability of NAC formation.

13

14

Abstracts

Calcareous nannofossil record of ODP Site 1090 (South
Atlantic) before and after the Eltanin impact at ~2.5Ma:
Preliminary results
Anne-Marie Ballegeer, José-Abel Flores, Francisco J. Sierro, Rainer Gersonde
The Eltanin asteroid impact was first discovered as an Ir
anomaly in 1981 (Kyte et al., 1981). The impact ripped up
Eocene, and probably Paleocene, sediments that afterwards
were redeposited in a chaotic assemblage (Gersonde et al.,1997). Chronostratigraphic data, obtained from a series of
4 piston cores recovered on the R/V Polarstern ANTXVII/5a Cruise, place the Eltanin impact at 2.5 Ma (Gersonde et al., 2003). It is the only known asteroid in a
deep-ocean basin. Recent results estimate that the asteroid
was larger than 1 km (Gersonde et al., 2003). Up to now,
no crater has been found. Glatz et al. (2002) claimed tohave found a 132 km crater, but this has been rejected lateron (Gersonde et al., 2003). The impact might have caused
mega-tsunamis, probably visible in sediments throughout
the Pacific and Southern Ocean shores, which may have
had an effect on the climate by ejection of large amounts ofsaltwater into the atmosphere (Gersonde et al., 1997). Disturbance from the impact clearly extends for about 100 km
north and east of the Freeden Seamounts. However, withincreasing distance to the north and the east, the concentrations of ejecta decrease and thick deposits of disturbed
sediments are not present (Gersonde et al., 2003).
In the last decade, scientists have tried to obtain a better understanding of the impact and its consequences. Impact deposits have been recovered from 20 sediment cores.
Tsunami deposits of 7-10 m thick, found along the coast of
N Chili, might be related to this impact (Felton & Crook,2003). A study of the sediment cores of the Bellinghausen
Sea, made by Flores et al. (2002), did not reveal significant changes in the calcareous plankton association for theinterval immediately after the impact, but relatively slow
sedimentation rates and extensive bioturbation may be indicative of paleoenvironmental changes immediately after
the impact. During Leg 178, Site 1096 (at 1300 km fromthe impact site) was examined to find traces of the impact.
In this site, no strong evidence was found that could be related to the impact (Kyte, 2001).
The present study is focused on the calcareous nannofossil record of this particular interval (between 3 and 2
Myr) to see whether or not significant changes in the calcareous nannofossil record can be observed and/or related
to the Eltanin impact. For this purpose, material of OPD
Hole 1090B, recovered during Leg 177, is studied. This
core is situated in the Subantarctic zone of the South Atlantic, on the southern flank of the Agulhas Ridge. A wellpreserved nannofossil assemblage is found, in which themost abundant species are Calcidiscus leptoporus, Coccolithus pelagicus, Reticulofenestra minuta and Reticulofenestra minutula. Strong fluctuations in the abundanceof these taxa are observed and may indicate oceanographic

changes during the Late Pliocene interval. It is difficult todetermine whether those changes could be related to the
Eltanin impact or to other important processes occurring
during this time interval (e.g., closure of the Isthmus ofPanama and the onset of Northern Hemisphere glaciation).
References
Felton, E.A.& Crook, K.A.W. 2003. Evaluating the impacts ofhuge waves on rocky shorelines: an essay review of the book
‘Tsunami - the underrated hazard’. Marine Geology, 197: 112.
Flores, J.-A., Sierro, F.J. & Gersonde, R. 2002. Calcareous plankton stratigraphy around the Pliocene “Eltanin” Asteroid Impact Area (SE Pacific): documentation and application forgeological and paleoceanographic reconstruction. Deep-Sea
Research, 49: 1011-1027.
Gersonde, R., Kyte, F.T., Bleil, U., Diekmann, B., Flores, J.-A.,
Gohl, K., Grahl, G., Hagen, R., Kuhn, G., Sierro, F.J., Völker,
D., Abelmann, A. & Bostwick, J.A. 1997. Geological recordand reconstruction of the late Pliocene impact of the Eltanin
asteroid in the Southern Ocean. Nature, 390: 357-363.
Gersonde, R., Kyte, F.T., Frederichs, T., Bleil, U. & Kuhn, G.
2003. New data on the late Pliocene Eltanin impact into thedeep southern ocean. Large meterorite impacts.
Glatz, C.A., Abbott, D.H. & Nunes, A.A. 2002. GSA Abstr. Prog.,
34(No.6): 401.
Kyte, F.T., Zhou, Z. & Wasson, J.T. 1981. High noble metal concentrations in a late Pliocene sediment. Nature, 292: 417-420.
Kyte, F.T. 2001. Data report: A search for deposits of the late
Pliocene impact of the Eltanin asteroid in rise sediments fromthe Antarctic Peninsula, Site 1096. In: P.F. Barker, A. Camerlenghi, G.D. Acton & A.T.S. Ramsay (Eds). Proceedings of
the ODP, Scientific Results, 178: 1-6.

Abstracts

15

Badenian calcareous nannoplankton from NE Slovenia(Mura depression, western Central Paratethys):
paleogeography and paleoecology
Milos Bartol
In the beginning of the Middle Miocene the Central
Paratethys reached its maximum extent. It consisted of aseries of larger and smaller epicontinental tectonic basins.
The Badenian corresponds to Langhian and Lower Serravallian of the Mediterranean and was the last fully marine
period in the life of Central Paratethys. It also corresponds
to the final stage of the Miocene Climatic Optimum(MCO), when favourable environmental conditions allowed for the thriving of diverse calcareous nannoplankton assemblages, producing a fossil record of great
biostratigraphic and paleoecological significance.
The Mura depression was one of the smaller basins near
the western coast of the Central Paratethys. Seventeen sections, composed of marls and subordinate sandstones,
sands and limestones were sampled. A few hundred samples were collected in 10 cm intervals for micropaleontological analyses. One hundred and seven species ofcalcareous nanoplankton and three species of calcisphere
were determined.
The diversity and abundance of nannoplankton allowed
a precise dating of individual sections and their correlation.
The total time span of the studied strata comprises the interval between the top of biozone NN4 in the early Badenian and the bottom part of biozone NN6 in the lateBadenian. This time interval was divided into six shorter
intervals. The oldest nanoplankton assemblages are assigned to the top part of biozone NN4, biozone NN5 contains four successive intervals, and the youngest interval
corresponds to the lower part of biozone NN6. The composition of nannoplankton assemblages and facies suggest
a heterogeneous nature of the Mura Depression, with deep
basins in immediate vicinity of shallow marine environments. This is clearly observable at the top of biozone NN5,
represented by marl beds with typically pelagic nannoplankton assemblages in one section and shallow-waterrhodoliths in several other sections only a few kilometresaway.
The pattern of biostratigraphic events observed in theyoungest nanoplankton assemblages, belonging at the beginning of the biozone NN6, is paleogeographically significant, since it is nearly identical to that described in the
Mediterranean (Fornaciari et al., 1996). The LO of Sphenolithus heteromorphus, the FO of Reticulofenestra
pseudoumbilica, the LCO of Cyclicargolithus floridanus
and the FO of Calcidiscus macroporus were observed inboth areas in the same succession. The first of these eventsis nearly synchronous on a global scale, while the others
are diachronous in different regions. The close resemblancein the character and the order of observed events indicatethat the Slovenian Corridor, a seaway between the Mediter-

ranean and the Central Paratethys, was still open in the beginning of the late Badenian (Fig. 1).

Figure 1: Paleogeographical sketch of the Mediterranean and the Central
Paratethys in the early late Badenian (modified after Rögl, 1998)

In the oldest nannoplankton assemblages (NN4), a
deepening trend was observed, reflecting a transgression at
the beginning of the Badenian. Younger assemblages fromthis interval are more diverse and contain several pelagic
species, which are absent in the oldest assemblages.
Throughout the entire biozone NN5, the high species diversity, abundance of Helicosphaera spp. coccoliths, andthe constant presence of rare specimens of sphenoliths anddiscoasters indicate relatively warm water. Some assemblages from the middle part of biozone NN5 and the ones
from the youngest strata (the upper part of NN5 and thebottom part of NN6) contain several dominant species (Helicosphaera carteri, Coccolithus pelagicus, Reticulofenestra minuta, R. spp.) as well as Reticulofenestra
pseudoumbilica and R. gelida (summer and winter varietyof the same species). This suggests increased seasonality
towards the top of the studied interval, which is in agreement with some published reports (Syabraj et al., 2007;
Bojar et al., 2004). Surprisingly, the warm-water characterof the youngest nannoplankton assemblages is very pronounced. An interval characterised by high diversity, enriched in the warm-water genera Discoaster andSphenolithus, was observed at the transition between biozones NN5 and NN6 at approximately 13.5 Ma. This iswell after the beginning of the drop in temperatures at theend of the MCO, which started at 14 Ma (Bojar et al., 2004;
Syabraj et al., 2007; Böhme, 2003). The enrichment in Discoaster spp., followed by an increase in abundance ofSphenolithus spp., closely resembles the pattern describedin the upper Badenian near Belgrade (Mihajlovic & Knezevic, 1989), and probably reflects the same event. The
nannoplankton assemblages from the Transylvanian Basin

16

Abstracts(Chira, 2001), belonging to the same interval, also show apattern similar to that recorded in Slovenia.
Late Badenian pollen and other terrestrial fossil plantsfrom the southernmost sites in Romania, Serbia and Hungary are characterized by thermophilous flora and indicate
subtropical climatic conditions, while a general cooling
trend appears in other Central Paratethys sites (Kvacek etal., 2006). The pattern of paleoclimatic changes in the Central Paratethys region at the end of the MCO has a regional
character. Perhaps, this was the result of a gradual termination of the connection between the Central Paratethys
and the Mediterranean that persisted in the westernmost
and the south-western parts of the region after it ended in
the others.
References
Böhme, M. 2003. The Miocene Climatic Optimum: evidence
from ectothermic vertebrates of Central Europe. Palaeogeography, Palaeoclimatology, Palaeoecology, 195: 389-401.
Bojar, A.V., Hiden, H., Fenniger, A. & Neubauer, F. 2004. Middle Miocene seasonal temperature changes in the Styrian
basin, Austria, as recorded by the isotopic composition of pectinid and brachiopod shells. Palaeogeography, Palaeoclimatology, Palaeoecology, 203: 95-105.
Chira, C. 2001: The Badenian calcareous nannoplankton from
Turda and Ocna Dej salt mines (Transylvanian basin, Romania). Studia Universitatis Babes-Bolyai, Geologia, 46(2): 141150.
Fornaciari, E., Di Stefano, A., Rio, D. & Negri, A. 1996. Middle
Miocene calcareous nannofossil biostratigraphy in the
Mediterranean region. Micropaleontology, 42(1): 37-62.
Kvacek, Z., Kovác, M., Kovar-Eder, J., Doláková, N., Jechorek,
H., Parashiv, V., Kovácová, M. & Sliva, L. 2006. Miocene
evolution of landscape and vegetation in the Central
Paratethys. Geologica Carpathica, 57(4): 295-310.
Mihajlovic, D. & Knezevic, S. 1989. Calcareous nannoplankton
from Badenian and Sarmatian deposits at Visnjica andKaraburma in Belgrade. Geoloski anali Balkanskoga poluostrva, Knjiga, 53: 343-366.
Rögl, F. 1998. Palaeogeographic considerations for Mediterranean and Paratethys Seaways (Oligocene to Miocene). Ann.
Naturhist. Mus., Wien, 99(A):279–310.
Syabryaj, S., Utescher, T., Molchanoff, S. & Bruch, A.A. 2007.
Vegetation and palaeoclimate in the Miocene of Ukraine.
Palaeogeography, Palaeoclimatology, Palaeoecology, 253:
153-168.

Abstracts

17

Dynamics of the surface-water masses in the North Atlantic
during the last 20 000 years as revealed by coccolithassemblages
Karl-Heinz Baumann, Helge Meggers
A coccolith-based micropalaeontological investigation of
ODP Sites 980 and 984 from the Feni and Gardar contour
drifts of the northern North Atlantic was conducted in orderto reconstruct the pattern and timing of surface circulation
changes in the area during the last 20 000 years. In addition,
sea-surface palaeotemperature records from both sites weregenerated at high resolution, based on the widely usedalkenone palaeothermometer.
The down-core variations in coccolith assemblage composition indicate that changes in properties of surface waters in the northern North Atlantic occurred stepwise during
the Termination I. Sparse occurrences of coccolithophores
before about 17 000 yrs BP at Site 980 and before about 13
500 yrs BP at Site 984, respectively, indicate harsh environmental conditions and the influence of melt-water. The
difference in timing between both sites is due to the position of the Polar Front, which was probably located between the site locations during the interval 17 000 to 13
500 yrs BP. The following stepwise increase of North Atlantic Drift water influence till about 10 000 cal yr BP was
associated with the increase in absolute numbers of coccolithophores in the whole area. High coccolith numbers
are observed in the early Holocene, which coincide wellwith maximum Northern Hemisphere summer insolation.
A cooling of the surface waters, as indicated by aprominent change in the relative abundances of the dominant coccolith species, occurred after about 5000 cal yr BP.
The numbers of the cold-adapted species Coccolithus
pelagicus increased considerably. In addition, a successive
increase in millennial-scale perturbations of the surface hydrology towards the Neoglaciation (the last ca. 5000 years)
is documented by changes in accumulation of the species,
in particular of Emiliania huxleyi. These successive decreases in the numbers of E. huxleyi, as previously described by Giraudeau et al. (2000), is in phase withrecorded Holocene advection of cool, ice-bearing watersfrom the Greenland-Iceland seas to the North Atlantic.
These long-term reorganisations of the surface hydrology
are interpreted as the response of the North Atlantic to the
combined forces of the solar insolation and the waning
Laurentide ice sheet.
Reference
Giraudeau, J., Cremer, M., Manthé, S., Labeyrie, L. & Bond, G.
2000. Coccolith evidence for instabilities in surface circulation south of Iceland during Holocene times. Earth Planetary
Science Letters, 179: 257-268.

18

Abstracts

Coccolith fluxes in the North Atlantic: Assemblage
composition and carbonate supply
Karl-Heinz Baumann, Claudia Sprengel, Harald Andruleit
Coccolithophores, one of the main primary producers inthe surface waters of the North Atlantic region, were investigated to quantify coccolith and coccolith-carbonate
export fluxes and to determine possible seasonal trends inspecies composition. Coccolithophore flux variations in
sediment traps at three mooring locations along an S-Ntransect at approx. 20˚W from 33˚N (L1) via 47˚N (L2) to55˚N (L3) were recorded from July 1995 to July 1997. The
20-cup particle traps were deployed at 1000m, 2000m, and3500m or 4000m below sea-surface; the material of the
2000m traps was studied. Sampling intervals ranged from
14 days to four weeks.
In general, total coccolith fluxes were characterized bya strong seasonality. Maximum coccolith flux values werereached in February-March (Station L1 at 33˚N) or JulySeptember (stations L2 and L3), respectively. Highest total
coccolith fluxes and fluxes of different species at the threesites were rather comparable. Surprisingly, the coccolith
fluxes at the relatively oligotrophic station L1 are up to 15
x 109 coccoliths m-2 d-1 and slightly higher than those at L2
and L3, where up to 5 x 109 coccoliths m-2 d-1 were observed. The examination of all trap samples revealed ahighly diverse coccolithophore assemblage with in total 63
species. Nevertheless, sinking assemblages at all sites are
dominated by E. huxleyi (generally >35%, >70% at L3),
with only F. profunda (at L1), Gephyrocapsa spp. (mainly
G. muellerae) and Syracosphaera spp. (at L3) contributing
considerably to the assemblages. All the other species exhibited maximum relative abundances of generally lessthan <10%.
In all trap samples, a conversion of coccolith fluxes into
coccolith-carbonate fluxes based on mean species-specificcarbonate masses was made. The mean contribution of coccolith-carbonate fluxes to the total carbonate fluxes in eachtrap was approx. 32%. The coccolith-carbonate fluxes are
dominated on the one hand by small-sized coccoliths of thedominant species E. huxleyi, on the other hand by thelarger, but less dominant, species C. leptoporus and C.
pelagicus.

Abstracts

Effect of ocean carbonate chemistry on Isochrysidales
calcification: studies from present and past oceans
Luc Beaufort
The calcite weight of Isochrysidales coccoliths andcoccospheres from samples taken in water and sediment
samples from the 3 oceans was estimated using automatedpattern recognition and automated morphometry software.
The calcite estimates made from more than 200 water
samples collected in the photic zone (more than 1000
individuals measured per sample) indicates that thevariability in the degree of calcification of Isochrysidales(weight of their coccoliths and coccospheres) strongly
depends on environmental parameters (alkalinity,
temperature and calcite saturation state). In areas of highalkalinity, high temperature, and high calcite saturation
state, the Isochrysidales secrete the heaviest coccospheres
and coccoliths. What is true at the order level(Isochrysidales) is also true at the species level for
Emiliania huxleyi but in a lesser degree because someregional differences occur for this species.
The Isochrysidales coccolith weight was estimated in
7 cores covering the last 40 kyr (3 from the Atlantic, 3 fromthe Pacific and 1 from the Indian Ocean) at the order andspecies (E. huxleyi) levels. All records exhibit highest
coccolith weight during the Last Glacial Maximum. When
all the records are stacked, the pattern of calcite weight
mirrors strongly that of the CO2 concentration in the
Vostock ice core. This cannot be due to dissolution for two
reasons: (1) dissolution in the Atlantic and Indo-Pacificoceans at the glacial/interglacial scale present opposite
histories; (2) laboratory experiments show little effect ofdissolution on the weight of the coccoliths. Therefore theweight variability observed at the Glacial/Interglacial timescale is the result of a change in the secretion of
Isochrysidales, certainly related to changes in theenvironmental parameters described in the modern ocean
study. Because the Last Glacial Maximum was obviously
not a time of higher oceanic temperatures, only changes in
the oceanic carbonate chemistry produced the observed
variations of Isochrysidales calcification. This study
provides a new case on the threat that the future increase inatmospheric CO2 and consequent ocean acidificationinduces on oceanic biological calcification.

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Abstracts

Campanian nannofossil biostratigraphy from Mississippi(Gulf of Mexico) and correlations to northwest Europe,
southwest France and Tunisia
James Bergen
Upper Santonian to lower Maastrichtian nannofossils investigated in the DCH-1 Foun Farms Corehole (Noxubee
County), and a composite of 14 outcrop sections from central Mississippi, demonstrate the potential in Campaniancalcareous nannofossil biostratigraphy and the possible significance of the Gulf Coast region in global correlation.
The exceptional preservation of recovered nannofossil assemblages and geographic-location-optimized biostratigraphic resolution; sample density and analysistime-limited results. Eighty Campanian nannofossil eventswere reproduced between the core and composite outcrop
section. Approximately 37 new species were observed inthis material, of which eleven were utilized for biostratigraphy. Lineages in the families Arkhangelskiellacae, Chiastozygaceae, Polycyclolithaceae, and Stephanolithiaceae
are presented.
The boundaries of the Campanian were constrained byanalyses of: (1) the Campanian/Maastrichtian GSSP section of Tercis les Bains, southwest France; and (2) Santonian/Campanian boundary sections in southern England(Whitecliff), Texas (Waxahachie), and Mississippi (Plymouth Bluff) containing the boundary fossil criterion, theextinction of the crinoid Marsupites testudinarius.
The Mississippi sections contain flora with both highand low-latitude affinities, but also many cosmopolitan
taxa. Latitudinal segregation first observed during the early
Campanian had become more severe near the close of theCampanian, making it difficult to correlate between sections in northwest Europe (southern England, Netherlands,
North Sea) and low latitudes (southwest France, Tunisia).
Nannofossil events in these eastern circum-Atlantic lowand high-latitude sections could be correlated to, and directly integrated within, the Mississippi succession.

Abstracts

21

Late Eocene to Oligocene preservation history andbiochronology of calcareous nannofossils from
paleoequatorial Pacific Ocean sediments
Teodora Blaj, Jan Backman, Isabella Raffi
A high resolution biochronologic study of late Eocene andOligocene calcareous nannofossils from a continuous carbonate sequence recovered at Ocean Drilling Program(ODP) Leg 199 Site 1218 in the paleoequatorial Pacific
Ocean led to the recognition of the following biohorizons:the highest occurrences (HO) of Discoaster barbadiensis(34.773 Ma), D. saipanensis (34.448 Ma), Ericsonia formosa (32.923 Ma), Reticulofenestra umbilicus (32.019

Ma), Sphenolithus predistentus (26.930 Ma), S. distentus(26.908 Ma) and S. ciperoensis (24.432 Ma), and the lowest occurrences (LO) of S. distentus (29.992 Ma) and S.
ciperoensis (27.093 Ma). In addition, the HO of S. predistentus was identified at 26.930 Ma, and the first consistentappearance of Triquetrorhabdulus carinatus occurs at
26.555 Ma, while the onset of the peak interval of T. carinatus was determined at 24.436 Ma. The stratigraphic

Figure 1: Plots of the range pattern of A) D. barbadiensis (thicker black line) and D. saipanensis (thinner black line), B) E. formosa, C) R. umbilicus.
Gray line represents carbonate content (weight %) in the panels. D) S. predistentus, E) S. distentus and the transitional form between S. predistentus
and S. distentus, F) S. ciperoensis and G) T. carinatus s.s. (black line) and T. aff. T. carinatus (gray line)22

Abstracts

Figure 2: The carbonate dissolution Intervals I – IV (34.63 Ma to 33.63 Ma): A) CaCO3%, the position of the E/O boundary and the time of the re-appearance of planktonic foraminifers (PF). Cumulative frequencies (in %) of complete (area left of heavy black line, with filled circles) versus broken(area right of heavy black line, with filled circles) specimens: B) E. formosa, C) R. umbilicus group, D) C. pelagicus, E) D. bisectus group, F) C. floridanus, G) total placoliths. H) Abundance (as cumulative %) of S. moriformis versus S. predistentus. I) Abundance of D. saipanensis versus D. deflandrei
and Discoaster spp. (0% D. saipanensis implies 100% of the D. deflandrei and the Discoaster spp. group, and vice versa)

range of Triquetrorhabdulus aff. T. carinatus has a duration of 3.3 Myr, representing the first complete range everdocumented for this morphotype. Information about thepreservation history of the selected species across the
Eocene/Oligocene boundary was achieved by investigating selected specimens and by studying the cumulative percentages of the complete versus broken specimens in theinterval between 34.63 and 33.63 Ma. Placolith preservation in this interval is controlled by the variation in the carbonate content values.

Abstracts

Evolutionary trends of selected coccolithophore species in
the North Atlantic during the Pliocene to Pleistocene
Babette Boeckel, Karl-Heinz Baumann, Elke Freytag, Markus Geisen
Selected keystone coccolith taxa, which are characterized
by a global distribution and a continuous geological record,
were quantified and morphologically analyzed. By meansof Plio- to Holocene Atlantic time-serie,s the range of theirmorphological variability is assessed to elucidate their evolutionary development. Geologic investigations on specieslevel diversity allow tentative concepts on speciation to betested, evaluated, and long-term patterns to be tracked, inorder to identify periods of niche differentiation. Special
attention is directed to interactions with biotic and abiotic
factors.
Selected coccolithophorid species from three
DSDP/ODP sites in the North Atlantic covering the last 5
Myr were biometrically characterized and the spatial distribution patterns of distinct morphotypes from the tropical
to northern NE Atlantic Ocean were reconstructed. Moreover, speciation and species evolution were evaluated withrespect to the decline and extinction events of other floral
elements.
The chosen time-interval, encompassing the Pliocene
to Quaternary, is characterised by significant geologic andclimate-relevant events: changes in oceanic and atmospheric circulation linked to the closing of the Isthmus ofPanama (4.6 Myr BP); the building up of the Northern
Hemisphere ice shields 3.1 Myr ago; the onset of enhanced
ice growth between 3.1 and 2.6 Myr BP, and finally the development of the Quaternary glacial-/interglacialcyclicity. A total of five species complexes wasquantitatively and morphologically analysed, including
Calcidiscus leptoporus, Florisphaera profunda, Syracosphaera pulchra, Umbilicosphaera sibogae and Coccolithus pelagicus.

23

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Abstracts

First data on oceanography, phytoplankton density andnutrient distribution of the western Libyan sea area
(August, 2006)
Sergio Bonomo, F. Azzaro, T. Bahri, G. Basilone, A. Bonanno, G. Buscaino, A.
Cuttitta, E. Di Stefano, O. Drebeka, A. Incarbona, M. Leonardi, A. Marini, F.
Massa, S. Mazzola, B. Patti, M. Talha, G. Tranchida, S. Zgozi
A multidisciplinary investigation was carried out in the sea
area in front of the western Libyan coast during August,2006. Hydrological data (CTD and ADCP), distribution ofnutrients (NO3, NH4, PO4), and phytoplankton and suspended matter (TSM, POC and PON) were collected during the MedSudMed-06 oceanographic survey, carried out
in the framework of the FAO Regional Project MedSudMed (“Assessment and Monitoring of the Fishery Re-

sources and the Ecosystems in the Straits of Sicily” fundedby the Italian Ministry of Agriculture Food and Forestry
Polices (MiPAAF), that promotes the scientific cooperation for fisheries research among four countries of the central Mediterranean - www.faomedsudmed.org). The main
aim of the survey was the study of the spatial distributionof the different life stages of small pelagic fish species inrelation to environmental parameters of the area, and inAbstracts

particular the correlations between chemical-physical andbiological parameters. Seventy-four water samples werecollected from different levels of the water column (5, 25,
50, 100, 150, 200, 500 m, bottom), in 14 stations. The interpretation of water-mass movements has been conductedusing both the current measurements of the LADCP and
the estimated geostrophic currents. The survey permitted
to get evidence on the displacement along the coast of typical Mediterranean waters (AW, ISW and LIW) moving in
opposite directions. The temperature profiles single out awell-developed thermocline at a mean depth of about 27
m, and a progressive decrease of temperature from about
28˚C at the surface to 13.6˚C near the bottom. The salinity
profiles evidence the AW (Atlantic Water) signature with aminimum (Smin) at about 75 m. The successive increase
reaches its maximum of salinity (Smax) at about 175 m(LIW core). Going deeper, both temperature and salinity
appear almost constant near the bottom, evidencing a homogeneous bottom layer of about 50-70 m thickness.
Phytoplankton quantitative analyses point out that, inthe summer period (August, 2006), the association is generally characterized by abundant diatoms and dinoflagellates, common to rare Coccolithophyceae and rare to veryrare silicoflagellates. A very high concentration of phytoplankton in the first 100 m is localized in the easternmost
part of the investigated area, near-shore. In this area, thedominant species is Leptocilindrus danicus. The dinoflagellate quantitative distribution shows high-density values(16 000 ~ 10 000 cell/l) in the first 25 m in the central-western zone. A lower concentration was found, near-shore, inthe western and eastern part of the area. Diatoms exhibit
very high-density values (400000 ~ 100000 cell/l) in thefirst 75 m in the easternmost part and a lesser density in thewesternmost area, near-shore. In general, diatoms are thedominant phytoplankton compound in the western Libyan
shelf. The coccolithophore quantitative distribution showsa gradual increase in the first 100 m of the western-central
zone (14000 ~ 2000 cell/l), and a rapid decrease in the central and eastern part (2000 ~ 400 cell/l density). A low to
middle degree of dissolution affects all calcareous phytoplankton species. The silicoflagellates, as expected, show
very low values and are confined to the deeper eastern andcentral zones. The recognized assemblage is constituted
only by Dictyocha fibula specimens that never reaches over
700 cell/l density.
Surface (0 - 25 m) concentrations of nitrate are elevated(~ 1.5 μM/l) in the transect in front of Tripoli, as well as in
the Zauara-Tripoli coastal area (> 1.5 μM/l, 25-60 m). The
vertical distribution of dissolved nitrate (1.48 ± 1.32 μM/l)shows an increasing trend with depth (max. 6.08 μM/l at
700 m). Nitrate and ammonia show, as expected, opposite
trends, in agreement with the recycling of respective nitrogenous compounds. The max. value of ammonia (4.68μM/l) was found at 5 m depth in the Zauara station. Valuesof reactive phosphate in the surface layer (5 m) are more elevated in the Zauara transect, as well as in the coastal station in front of Tripoli (~ 0.6 μM/l). The PO4 vertical

25

distribution does not appear regular in several investigatedstations (PO4 0.38 ± 0.19 μM/l). The phosphorous and ammonia increments recorded in the Zauara coastal area areprobably due to urban discharges. On the other hand, therelatively high nitrate concentration in the coastal Tripoli
area could be interpreted as a consequence of agriculture
activities, possibly using nitrogen fertilizers. The incidenceof Total Suspended Matter (TSM) was high in all considered samples, ranging between 7.60 and 19.65 mg/l. POC
and PON are not elevated, but higher than those found inprevious investigations in the Strait of Sicily. Higher POC
values (>150 μgC/l) were registered in the euphotic layer(max. = 235.60 μgC/l) overall in the off-shore area, whilein the near-shore they were generally lower. The C/N ratio
values show a general condition of equilibrium between
the trophic components (autotrophy, heterotrophy, detritus). In surface waters, a better efficiency level of the autotrophic compartment was found in the easternmost area,
where C/N values ranged between 6 and 8. However, in theoff-shore area in front of Tripoli, higher C/N ratio values
suggest that the phytoplankton community is not very efficient (C/N > 9).

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Abstracts

Morphological similarities linking fossil species E. macellus
to the extant coccolithophorids Gaarderia andUmbellosphaera: Significant implications for the function of
coccoliths
David Bord, Marie-Pierre Aubry
The coccolithophorids are a group of phytoplankton that
secretes a carbonate shell called a coccosphere. The lattercomprised interlocking mineralized scales called coccoliths. In the extant coccolithophorids, there are, in general,
little morphologic differences among coccoliths on individual coccospheres. Two notable exceptions are thespirothecate coccospheres of Gaarderia and Umbellosphaera. In them, the larger, external coccoliths have abroad marginal cycle and a narrow central cycle; thesmaller, inner coccoliths are structurally opposite. Aroundthe spirothecate, there is a gradual modification of the morphology as size increases. Thus size variations of sedimented coccoliths of these genera are not simply indicativeof species differences, but reflect the composition of coccospheres.
The coccoliths of one fossil species, Ellipsolithus macellus, show a large morphologic variability. The coccolithsof E. macellus are very delicate, and no intact coccosphere
has been recovered. It is possible that this variability reflects the co-existence of several species under one paleontological name. But it is also possible that it reflects theoriginal composition of the coccosphere, with coccoliths
of different shapes and sizes forming a spirothecate coccosphere, analogous to that of Gaarderia and Umbellosphaera. Although of different basic structures, themorphology of the coccoliths of E. macellus are strongly
reminiscent of those of Gaarderia and Umbellosphaeraspp.
I have conducted a quantitative analysis on over 400
specimens of E. macellus from the lower Paleocene of
Egypt, measuring and analyzing variations in the dimensions of coccoliths. I have done the same with publishedfigures of Gaarderia and Umbellosphaera. The preliminary conclusions of this work are that the coccosphere of E.
macellus may well have been spirothecate. The function of
the coccoliths is still unknown, although several ideas havebeen offered, including protection, flotation, and/or the regulation of light (Young, 1994). A new function for severalof the specialized coccolith groups, including Gaarderia
and Umbellosphaera, has been proposed: these coccoliths
may be highly specialized for food collection, which would
possibly suggest mixotrophy among at least some extant
coccolithophorids (Aubry, in press). If this is the case, morphologic variation in E. macellus may be indicative of
mixotrophic physiology.
References
Aubry, M.-P. In press. A Sea of Lilliputians. Palaeogeography,
Palaeoclimatology, Palaeoecology.

Young, J. 1994. Function of coccoliths. In: A. Winter, A. & W.G.
Siesser (Eds). Coccolithophores. Cambridge University

Press, Cambridge: 63-82.

Abstracts

Applying statistical techniques to construct a refined
Paleocene-Eocene calcareous nannofossil biozonation
Andrew R. Bowman, David K. Watkins, Felix M. Gradstein
In an effort to refine the resolution of the existing Paleocene-Eocene calcareous nannofossil biostratigraphic
zonations, a statistically rigorous methodology was applied
to various deepwater sections. Abundance counts on calcareous nannofossils were performed on two ODP sites(Leg 171B, Sites 1051A and 1052A, Blake Nose), and ona deepwater Gulf of Mexico well (Keathley Canyon, Block774, “Ponza”). In addition, calcareous nannofossil biostratigraphic data were taken from published work, and incorporated into this study to increase the dataset size. Afterthe abundance counts were performed and the data werecompiled, a detailed evaluation of the many hundreds ofPaleogene-age taxa was carried out, using hardcopies of
species distribution charts (BugCAD plots), followed byanalysis of results processed through specialized computer
software (IPS). This process yielded the placement of themore common types of bioevents (i.e., species range tops
and bases), and in addition aided in the recognition of new,useful, subordinate bioevents (e.g., first downhole increases). All bioevents were then analyzed using the ranking and scaling probabilistic sequencing method (RASC).
The RASC method resulted in the most probable order,
termed the “optimum sequence”, for the Paleocene-Eocene
calcareous nannofossil bioevents. With the possible discovery of new, non-traditional bioevents, and resulting increased biostratigraphic resolution, the produced optimum
sequence has the potential to aid in the success of biostratigraphic correlation within key hydrocarbon fields, aswell as between geographically widespread basins.

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Abstracts

Calcareous nannoplankton evolution and the Paleocene/
Eocene thermal maximum event
Paul Bown, Tom Dunkley Jones
Calcareous plankton are ideally suited to the assessment of
evolutionary change through past rapid climate change
events because they are abundant, widespread and cosmopolitan organisms. The study of these fossils has been integral to our recognition and emerging understanding of
the Paleocene/Eocene thermal maximum (PETM), which is
now a major focus of attention as an historic example of acarbon cycle event comparable to that predicted for the
next century, i.e., rapidly increasing atmospheric CO2,
global warming and possible ocean acidification. The
PETM geological record has provided unambiguous evidence of disruption in the deep-sea environment, with acidification and large temperature rises accompanied byelevated extinction rates in benthic foraminifera. Evidenceof similar disruption in the surface ocean plankton, however, currently comprises observations of poleward migration, short-lived ‘excursion taxa’ and elevated evolutionary
turnover in calcareous phytoplankton. This is a somewhat
muted evolutionary response, considering the temperature
and acidification effects that have been proposed for thisinterval. Here we examine whether this evidence may becompromised by the quality of the stratigraphic and fossil
record by analysing plankton from an expanded,hemipelagic PETM section in southern Tanzania (Tanzania Drilling Project Site 14) that, in background conditionsat least, provides exceptionally preserved calcareous microfossils and therefore the optimal prospect of recovering
reliable assemblage and diversity data. The calcareous
nannoplankton are more diverse than any previously documented sections of the same age, and include small andfragile taxa that are not present in ‘normal’ preservation
states. The PETM onset is marked by rapid and significant
nannoplankton assemblage shifts, reduction in abundanceand diversity, and synchronous extinctions representing
around 10% of the total diversity. These changes clearly
indicate severe disruption of the photic zone environment,
but the disappearing taxa reveal no strong extinction selectivity bias and the assemblage shifts are not easily explained by the effects of dissolution, dilution, or
productivity. Diagnostic nannoplankton components areobserved throughout the carbon isotope excursion interval,
but are replaced above this level by assemblages that are remarkably similar to those seen prior to the event. Despite
synchronous extinctions at the PETM onset, and significantly perturbed assemblages for the duration of the PETM
event, the plankton underwent only minor evolutionarychanges in the longer term. Nevertheless, the event fellwithin the interval that saw the highest turnover rates in thehistory of the calcareous nannoplankton group.

Abstracts

Coccolithophore calcification: cellular mechanisms andconstraints
Colin Brownlee, Abul Chrachri, Glenn Wheeler, Alison Taylor
We are adopting a combined cell physiological and genomics approach to understand the cellular mechanisms ofcalcification in coccolithophores. This work is uncoveringsome unexpected pathways and mechanisms. In the longer
term, our aim is to genetically manipulate specific components of the process to understand their function. An understanding of these mechanisms, and how they vary in
different coccolithophore species, will hopefully improve
our ability to predict how coccolithophore populations may
be affected by, or adapt to, changing ocean chemistry inboth the short and long term.

29

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Abstracts

Review of calcareous nannofossil biostratigraphy andbiochronology for the upper Miocene-Pliocene at ODP Site
999 (Caribbean Sea)
Margarita Buitrago-Reina, José-Abel Flores, Francisco J. Sierro, Vladimir Torres
Torres
Ocean Drilling Program (ODP) Site 999A was drilled by
the R/V Joides Resolution during Leg 165 in the Caribbean
Sea. This site is located in the Colombian Basin(12˚44.639’N, 78˚44.360’W), on a promontory named
Kogi Rise, or Chibchas Rise, at a water depth of 2827.9 m(Sigurdsson et al., 1997). The calcareous nannofossil biostratigraphy at Site 999A was previously studied by Kameo& Bralower (1997), using bioevent data for the upper
Pliocene and Pleistocene (Raffi & Flores, 1995; Takayama
et al., 1995) and zonal schemes for the Neogene and the
Quaternary (Martini, 1971; Bukry, 1973, 1975; Okada &Bukry, 1980). This study provided a low-resolution biostratigraphic scheme. Due to this, the main aim of this work
is to achieve a high-resolution biostratigraphic andbiochronologic record over the Upper Miocene to Pliocene.
We have prepared 298 samples, with an average spacing of between 3 cm to 24 cm. The slides were preparedfollowing a decantation technique (Flores & Sierro, 1997)
and they were analysed using a polarized microscope at amagnification of 1000x. Calcareous nannofossils show
good to moderate preservation throughout the studied
stratigraphic interval. Evidence of reworking is recordedby the finding of specimens like Lithostromation perdurum, with an age range from Late Paleocene to Early
Eocene. The identification of some calcareous nannofossil
markers allowed the recognition of the biozones proposedby Martini (1971) and Okada & Bukry (1980). The Upper
Miocene (Biozone NN10; Okada & Bukry, 1980) is defined in this study by the first ocurrence (FO) datum of
Reticulofenestra rotaria, which appears approximately at
239.1 mbsf with an average age of 8.76 Ma. Additionally,
the FO datums of Discoaster berggrenii at ~229.65 mbsf,
Amaurolithus primus and Catinaster mexicanus (both at
229.5 mbsf) were used to locate the boundary between Biozones CN8/CN9 (Okada & Bukry, 1980) and NN10/NN11(Martini, 1971). Magnetostratigraphic and oxygen and carbon stable isotope records measured in Site 999 will further
improve the biochronology of this site.
References
Bukry, D. 1973. Low-latitude coccolith biostratigraphic zonation.
Initial Reports of the Deep Sea Drilling Project, 15: 685-703.
Texas A & M University, Ocean Drilling Program, College
Station, TX, United States.
Bukry, D. 1975. Coccolith and silicoflagellate stratigraphy,
northwestern Pacific Ocean, Deep Sea Drilling Project, Leg
32. Initial Reports of the Deep Sea Drilling Project, 32: 677701. Texas A & M University, Ocean Drilling Program,College Station, TX, United States.
Flores, J.-A. & Sierro, F.J. 1997. Revised technique for calcula-tion of calcareous nannofossil accumulation rates. Micropaleontology, 43: 321-324.
Kameo, K. & Bralower, T.J. 1997. In: H. Sigurdsson, R.M.
Leckie, G.D. Acton et al. (Eds). Proceedings of the Ocean
Drilling Program, Scientific Results, 165: 3-17. College Station, TX (Ocean Drilling Program)Martini, E. 1971. Standard Tertiary and Quaternary calcareous
nannoplankton zonation. In: A. Farinacci (Ed.). Proceedingsof the II Planktonic Conference, Roma, 1970, 2: 739–785.
Okada, H. & Bukry, D. 1980. Supplementary modification andintroduction of code numbers to the low-latitude coccolith
biostratigraphic zonation (Bukry, 1973; 1975). Marine Micropaleontology, 5: 321–325.
Raffi, I. & Flores, J.-A. 1995. Pleistocene through Miocene calcareous nannofossils from the eastern equatorial Pacific
Ocean. Proceedings of the Ocean Drilling Program, Scientific Results, 138: 233-286. College Station, TX (Ocean
Drilling Program).
Sigurdsson, H., Leckie, R.M., Acton, G.D. et al. 1997. Proceedings of the Ocean Drilling Program, Scientific Results, 165:
335pp. College Station, TX (Ocean Drilling Program).
Takayama, T., Sato, T., Kameo, K. & Goto, T. 1995. Quaternary
coccolith biostratigraphy and the age of the Pliocene/Pleistocene boundary. Quaternary Research, 34: 157–170.

Abstracts

31

Multivariate Morphon Analysis of Braarudosphaera bigelowii
during a Holocene interval at Mira (SW Portugal)
Mário Cachão, Ana Bento, Conceição Freitas, Aurea Narciso
Morphometric analyses of Braarudosphaera bigelowii
have already been performed by several authors (seeTakano et al., 2006). Applying slightly distinct methods,
all concluded for the existence of several morphotypes. The
question of their specific behaviors and (paleo)ecologicalmeaning, however, remained to be addressed most of thetime.
With the Multivariate Morphon Analysis (MMA; Parente et al., 2004; Narciso et al., 2006), one can test on aparticular calcareous nannofossil taxon for the existence ofdistinct morphotypes, with the additional advantage that,simultaneously, their individual behaviors are also described and characterized, opening a door for the understanding of their potential use as individual paleoecologicalproxies (see Narciso et al., 2006).
For the present study, a Holocene section of a core retrieved from the present-day Mira estuary (SW Portugal)
was selected due to its abnormal abundance of pentaliths of
B. bigelowii during an estimated time interval of 2.5 ky, between 8.5 and 6.0 14C yrs cal BP, when the region was aformer paleo-ria (Alday et al., 2006).
MMA results suggest the existence of 5 distinct morphotypes, each defined by a particular size interval and a
specific behavior along the selected core section. The
measurement method, morphotypes, and their paleoecological significance will be presented and discussed.
References
Alday, M., Cearreta, A., Cachão, M., Freitas, M.C., Andrade, C.
& Gama, C. 2006. Micropaleontological record of Holocene
estuarine and marine stages in the Corgo do Porto rivulet(Mira River, SW Portugal). Estuarine, Coastal and Shelf Science, 66: 532-543.
Narciso, A., Cachão, M. & de Abreu, L. 2006. Coccolithus pelagicus subsp. pelagicus versus Coccolithus pelagicus subsp.
braarudii (Coccolithophore, Haptophyta): a proxy for surface
subarctic Atlantic waters off Iberia during the last 200 kyr.
Marine Micropaleontology, 59: 15-34.
Parente, A., Cachão, M., Baumman, K.-H., de Abreu, L. & Ferreira, J. 2004. Morphometry of Coccolithus pelagicus s.l.
(Coccolithophore, Haptophyta) from offshore Portugal, during the last 200 kyr. Micropaleontology, 50 (Supplem 1): 107120.
Takano, Y., Hagino, K., Tanaka, Y., Horiguchi, T. & Okada, H.
2006. Phylogenetic affinities of an enigmatic nannoplankton,
Braarudosphaera bigelowii based on the SSU rDNA sequences. Marine Micropaleontology, 60(2): 145-156.

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Abstracts

Paleoenvironmental changes in a Kimmeridgian platform(western France) revealed by calcareous nannoplankton
and ascidian spicule variations
Damien Carcel, Fabienne Giraud, Claude Colombié
The Kimmeridgian carbonate ramp environments ofwestern France are characterized by limestone-marlalternations with abundant storm deposits. Different ordersof cyclicities were recognized in these deposits, revealinga climatic control of the sedimentation linked to changes
in orbital cycles. The aim of this work is to study the
paleontological content of autochthonous marl-limestone
deposits in order to reconstruct paleoenvironmental
changes prevailing during the Kimmeridgian. The
carbonate fraction was examined in the field and in thinsections for macro- and microfossils, and the fine carbonate
fraction was studied in smear slides for calcareous
nannofossils. Smear slides were prepared following therandom settling method of Geisen et al. (1999) in order tocalculate absolute abundance. The essential component of
the carbonate fraction is mud. The coarse carbonate
fraction, which is minor, is composed of benthic organisms(bivalves, echinoderms, agglutinated foraminifers andgastropods). Macro- and microfossils observed are
ubiquitous organisms, and do not allow determination of
precise paleoenvironmental conditions. The fine carbonate
fraction is constituted of three types of calcareous
nannofossils (ascidian spicules, coccoliths andschizospheres). Calcareous nannoplankton and ascidian
spicules were counted separately. The ascidian spicules,
which were attributed in a preceeding work to the genius
Didemnum (Busson et al., 1996), are the dominant
contributor. The total abundance of calcareous nannofossils(ascidian spicules and calcareous nannoplankton) is
negatively correlated with the calcium carbonate content.
However, in marls, ascidian spicules constituted the majorpart of the fine carbonate fraction. According to Brookfield(1988), ascidians are important members of shallow-water
benthic communities. They are rarely described in ancient
sediments, and in particular in the Mesozoic. Busson et al.
(1996) considered that they may not have been recognized,or misinterpreted as calcareous nannofossils. A recent study
has shown that ascidian spicule variations were linked tosurface-water productivity, revealing the importance of thisgroup in paleoceanographical reconstructions (Toledo etal., 2007).
Among the calcareous nannoplankton recognized in the
Kimmeridgian
limestone-marlalternations,theassemblages are dominated by the small placoliths of
Watznaueria (in particular, small morhotypes of W.
britannica described in Giraud et al., 2006) andCyclagelosphaera margerelii. Schizospheres, whenpresent, are characterized by small sizes (between 5 and 8μm). The decrease through the Kimmeridgian in the
Watznaueria/Cyclagelosphaera ratio suggests more

proximal conditions, or progradation of the carbonate
platform, in the Late Kimmerdigian, with respect to the
Early Kimmerdigian. The variations of the nannofossil
assemblages (calcareous nannoplankton) and benthic
community (represented here by ascidians) through theKimmeridgian are indicative of variable trophic levels,
related to changes in climatic conditions.
References
Busson, B., Noël, D., Monniot, F. & Cornée, A. 1996. Attribution
de corpuscules calcaires observés dans des marnes duJurassique supérieur à des spicules du genre Didemnum(Ascidie, Tunicier). In: F.G. Bourrouilh-le Jan (Ed.).
Carbonates intertropicaux. Mém. Soc. géol. France, n.s., 169:
145-154.
Geisen, M., Bollmann, J., Herrle, J.O., Mutterlose, J. & Young,
J.R. 1999. Calibration of the random settling technique forcalculation of absolute abundances of calcareous nannoplankton. Micropaleontology, 45: 123-138.
Giraud, F., Pittet, B., Mattioli, E. & Audouin, V. 2006. Paleoenvironmental controls on morphology and abundance of thecoccolith Watznaueria britannica (Late Jurassic, southern
Germany). Mar. Micropaleontol., 60: 205-225.
Toledo, F.A.L., Cachão, M., Costa, K.B. & Pivel, M.A.G. 2007.
Planktonic foraminifera, calcareous nannoplankton andascidian variations during the last 25 kyr in the Southwestern
Atlantic:A
paleoproductivity
signature?
Mar.
Micropaleontol., 64: 67-79.

Abstracts

33

Calcareous nannofossil and calpionellid calcification events
across the Tithonian-Berriasian time-interval and lowlatitude paleoceanographic implications
Cristina Emanuela Casellato, Gloria Andreini, Elisabetta Erba, Guido Parisi
Calcareous nannofossil and magnetic stratigraphies of several sections spanning the Middle-Upper Jurassic to lowermost Cretaceous have been studied in the Lombardian
Basin (Torre di Busi, Colle di Sogno) and Trento Plateau(Colma di Vignole, Foza, Frisoni, Sciapala, Bombatierle,
Passo Branchetto) in order to integrate calcareous nannofossil events with the polarity chron sequence and, whereavailable, with calpionellid biostratigraphy. Calcareous
nannofossil biostratigraphy has been carried out on smear
slides prepared from un-heated end-pieces of the same
samples used for magnetostratigraphy. Similar variationsin nannofloral abundance and composition have been documented in all sections. In the Jurassic/Cretaceous boundary time-interval, all previously-known calcareous
nannofossil zones and corresponding subzones (Bralower
et al., 1989) have been clearly recognized. In the CallovianKimmeridgian interval, a tentative integration of biostratigraphy (De Kaenel et al., 1996; Bown, 1998;
Cobianchi, 2002) with polarity chrons is proposed. The
magnetic stratigraphies span the CM16R (late Berriasian)to the CM25 (Oxfordian) interval. The identification of polarity zones is based on polarity-zone pattern fit, and, whereavailable, on the previously-established correlations of polarity chrons to nannofossil events/zones (Channell &Grandesso, 1987; Channell et al., 1987; Weissert & Channell, 1989; Bralower et al., 1989).
References
Bown, P.R. & Cooper, M.K.E. 1998. Jurassic. In: P.R. Bown
(Ed.). Calcareous Nannofossil Biostratigraphy. British
Micropalaeontological Society Publications Series. Kluwer
Academic Publishers, London: 34-85.
Bralower, T.J., Monechi, S. & Thierstein, H.R. 1989. Calcareous
Nannofossil Zonation of the Jurassic-Cretaceous Boundary
Interval and Correlation with the Geomagnetic Polarity
Timescale. Marine Micropaleontology, 14: 153-235.
Channell, J.E.T., Bralower, T.J. & Grandesso, P. 1987.
Biostratigraphic correlation of M-sequence chrons at Capriolo
and Xausa (S. Alps, Italy). Earth Planetary Science Letters,
85: 203-221.
Channell, J.E.T., Erba, E., Nakanishi, M. & Tamaki, K. 1995. Late
Jurassic-Early Cretaceous time scales and oceanic magnetic
anomaly block models. Geochronology Time Scale andGlobal Stratigraphic Correlation, 54: 51-63.
Channell, J.E.T. & Grandesso, P. 1987. A revised correlation of
Mesozoic polarity chrons and calpionellid zones. Earth
Planetary Science Letters, 85: 222-240.
Cobianchi, M. 2002. Calcareous nannofossils from the Middle
and Upper Jurassic of the Belluno Basin (Southern
Calcareous Alps). Atti Ticinensi di Scienze della Terra, 43: 324.
De Kaenel, E., Bergen, J.A. & Perch-Nielsen, K. 1996. Jurassic
calcareous nannofossil biostratigraphy of Western Europe.

Compilation of recent studies and calibration of bioevents.
Bulletin Société geologique de France, 167(1): 15-28.
Weissert, H. & Channell, J.E.T. 1989. Tethyan carbonate carbon
isotope stratigraphy across the Jurassic/Cretaceous boundary:an indicator of decelerated global carbon cycling?
Paleoceanography, 4(4): 483-494.

34

Abstracts

New bio-magnetostratigraphy for the Upper Jurassic andlowermost Cretaceous of the Southern Alps (Italy)
Cristina Emanuela Casellato, Elisabetta Erba, James E.T. Channell, Giovanni
Muttoni
The Tithonian-Berriasian time interval is characterized bya major calcareous nannofossil speciation episode and by
the appearance of the calpionellid group: several generaand species first appear and evolve, showing an increase indiversity, abundance and particularly in calcification degree. This time interval is also characterized by a significant, low-latitude increase of carbonate-rich sediments(Rosso ad Aptici Fm. toward Maiolica Fm.).
Calcareous nannofossil and calpionellid biostratigraphy
and absolute abundances have been performed on low-latitude selected sections in order to reconstruct biogenic calcite palaeofluxes. Calpionellids have been investigated onthin sections (25mm thick), while calcareous nannofossilon the same, but thinner, thin sections (up to 7μm thick)used for the calpionellids. All specimens have been counted
on 1 cm2 of thin section or 1 mm2 of ultra-thin section, respectively, for calpionellids and calcareous nannofossils.
Paleofluxes have been obtained, integrating absolute abundance with single speciment mass weight (10-12g of calcareous carbonate) per area unit (cm2) per time unit (yr).
Calcareous biogenic paleofluxes point out a link between the lithologic changes and calcified plankton evolution across the Tithonian-Berriasian interval. During theLower Tithonian (Rosso ad Aptici Fm.), a first calcification event is characterized by a nannolith (F. multicolumnatus, C. mexicana, P. beckmannii) increase in abundance,
size and calcification degree, followed by the occurrence ofthe first calcified calpionellid (Tintinopsella). Across theUpper Tithonian to Lower Berriasian (Rosso ad Aptici Fm.Maiolica transition and Maiolica Fm.), a second bigger calcification event is characterized by a dramatic increase of
nannoconid abundance and calcification degree, reaching
lithogenetic amounts, concomitant with a moderate abundance increase of calcified calpionellid (genera Crassicollaria, Calpionella, Remaniella).
Linkages between calcareous nannofossil and calpionellid evolution with geologic, palaeoceanographic or
palaeoclimatic events are inferred. The diversification andbiomineralization of highly-calcified plankton produced amajor increase in pelagic carbonate sedimentation due tothe onset of paleoenvironmental conditions favorable tocalcification. The diversification and proliferation of nannoliths and nannoconids, interpreted as inhabitants of thelower photic zone, might indicate the establishment of athermocline/nutricline in the deep photic zone, suggesting
the development of oligotrophic and stable oceanic conditions.
It is also suggested that Tithonian-Berriasian calcified
plankton evolution could be controlled by a decrease in
pCO2, due to a decreased spreading rate and/or increased
weathering rate (87Sr/86Sr) and cool climatic conditions,concomitant with a decrease in the oceanic Mg/Ca ratio
values. Both factors thermodynamically promoted low MgCaCO3 and CaCO3 biomineralization, supporting calpionellid and calcareous nannofossil abundance andcalcification rate increases.

Abstracts

35

Cretaceous and Paleogene calcareous nannofossils from
northern Moldavia (Sucevita-Putna area, Romania) and theCretaceous/Paleogene Boundary
Carmen Mariana Chira, Ramona Balc, Alin Igritan, Florin Florea
Detailed biostratigraphic data are presented here in order toinvestigate the K/P boundary from northern Moldavia (Bucovina). The sections studied for establishing Cretaceousand Paleogene calcareous nannofossil biostratigraphy arelocated in the Sucevita – Putna area, and in the Bercheza,
Rusca and Putna valleys. Previous, preliminary data concerning a part of this area were presented by Chira et al.
(2007).
The studied area comprises three tectonic units, fromeast to west: Pericarpathian, Vrancea and Tarcau, with complex geological structures. The investigated sections belong to the Hangu (Upper Cretaceous), Izvor (Paleocene Lower Ypresian) and Straja Formations (Middle Ypresian).
These formations are part of the Tarcau Nappe (Upper Cretaceous - Oligocene).
In the Sucevita Basin, previous studies on the K/Pboundary have been carried out by Ionesi (1975) andIonesi & Florea (1984, 1996). The K/P boundary was identified in the upper part of the Formation with Inoceramids(Ionesi & Florea, 1996), or upper part of the Hangu Formation in the Tarcau Nappe (Juravle, 2007).
The Izvor Formation from the Sucevita - Putna area was
assigned to NP5-NP9 (Paleocene) and NP10-11 (Lower
Eocene) (Ionesi & Florea, 1996). The calcareous nannofossil assemblages from the Sucevita and Bercheza valleys
contain, among others: Disco. salisburgensis, D. binodosus, D. lodoensis, D. distinctus, Chiasmo. solitus, Tribrach. orthostylus, Cocco. formosus, Helico. lophota,
Chiasmo. grandis, which indicate a Cuisian age. The assemblage with D. binodosus, D. lodoensis, C. solitus, C.
formosus, C. grandis, Towe. pertusus was assigned to NP12
(middle Ypresian). The assemblage with D. lodoensis, C.
formosus, C. grandis, H. lophota, Retic. dictyoda, Spheno.
moriformis belong to NP12-13 (middle Ypresian). These
two biozones were identified also in the samples from
Rusca Valley.
Studies on the K/P boundary were performed by
Melinte (2000) and Bojar et al. (2007) in the southern partof Moldavia, where was remarked the presence of Upper
Maastrichtian/Lower Paleocene deposits, thanks to theidentification of the biozones Neph. frequens, Mic. prinsii,
Biantho. sparsus and Cruci. primus. The K/P deposits from
northern Moldavia, and the boundaries between formationsof different ages, are usually in tectonic contact.
In Bercheza Valley, in the Sucevita area, Upper Cretaceous deposits contain: Mic. staurophora, Arkh. cf. A.
maastrichtiana, Watz. barnesiae, Cribro. ehrenbergii, Calc.
obscurus, Luc. cf. L. windii and L. maleformis. The Paleogene deposits comprise: Disco. saipanensis, Black. pinguis,Thoracosphaera sp.

In the Sucevita area, along the Rusca Valley, the Upper
Cretaceous samples contain: Predisco. cretacea, M. staurophora, Arkh. sp., Micro. decoratus, L. maleformis, Rete.
crenulata, Eiff. eximius, Rein. levis, Stauro. sp., Trano. orionatus, W. barnesiae, Uniplan. gothicus, Broin. parca constricta. The Paleogene deposits comprise frequent D.
lodoensis, D. saipanensis, D. binodosus, D. elegans andalso T. ortostylus, Spheno. radians, S. pseudoradians, Helico. cf. H. recta, H. bramlettei, Cocco. pelagicus, Towe.
rotundus, Chias. gigas, Trans. cf. T. latus and T. pulcher.
In the Putna Valley were found Upper Cretaceous assemblages with Cerato. sesquipedalis, C. arcuatus, C. quasiarcuatus, L. maleformis, Arkh. cymbiformis, Eiff.
turriseiffelii, M. staurophora, W. barnesiae, Zeug. scutula.
The Paleogene deposits contain: B. sparsus, B. haqii, C.
pelagicus and Retic. umbilica.
In the sections from the Rusca and Bercheza valleys,
generally assemblages are poorly preserved, with fragmentation and overgrowth. Better-preserved and moreabundant assemblages were identified in the Putna Valley.
Alternation of Upper Cretaceous and Paleogene deposits
was observed, due to the tectonics of the region.
References
Bojar, A.-V., Melinte. C.M. & Bojar, H.-P. 2007. The environmental and tectonic record of a continuous Cretaceous/Paleogene section from the Eastern Carpathians. Abstracts,
Proceedings of the European Society for Isotope Research,
ESIR IX. Studia Universitatis Babes-Bolyai, Geologia, 52(1):7-8.
Chira, C., Balc, R., Igritan, A. & Florea, F. 2007. Cretaceous –Paleogene calcareous nannofossil assemblages from Sucevita– Putna area: Bercheza, Rusca and Putna Valleys (northern
Moldavia), and the problem of the Cretaceous/Paleogene
Boundary. Abstract, Annual Scientific Session, Departmentof Geology, Cluj-Napoca.
Ionesi, L. 1975. Limite Maestrichtien-Paleocene et Cuisien Nummulitique dans le flysch de Bucovine. Micropaleontological
Guide to the Mesozoic and Tertiary of the Romanian
Carpathians. Excursion L. Bucharest: 145-154.
Ionesi, L. & Florea, F. 1984. Quelques aspects concernant lalithostratigraphie et la structure du flysch externe du Bassin dela Sucevita. Analele stiintifice ale Universitatii Al. I. Cuza din
Iasi, 30: 5–12.
Ionesi, L. & Florea, F. 1996. Contributii litostratigrafice si sedimentologice asupra Formatiunii cu Inocerami (Hangu s.s.).
Studii si cercetari de geologie, 41: 81–92.
Juravle, D.T. 2007. Geologia regiunii dintre Valea Sucevei si
Valea Putnei (Carpatii Orientali). Casa Editoriala Demiurg,
Iasi: 6-319.
Melinte, M. 2000. Cretaceous/Tertiary boundary in the East
Carpathians, based on nannofloral evidence. Acta Paleontologica Romaniae, 2: 269-273.

36

Abstracts

The Paleogene/Neogene boundary in northern Moldavia(Moldovita Basin, Romania)
Carmen Mariana Chira, Doru Toader Juravle, Ramona Balc, Alin Igritan, Mirela
Violetta Popa
The Paleogene/Neogene boundary in the External Flysch
area of the Eastern Carpathians (Northern Moldavia) constituted for a long time the topic of a controversial and intense scientific debate. Calcareous nannofossils werepreviously studied from other basins, situated south of the
Moldovita Basin: the Tarcau (Martini & Lebenzon, 1971;
Lebenzon, 1973), Tazlau (Ionesi & Gheta, 1978; Dicea &Dicea, 1980) and Buzau Basins (Melinte, 1988).
The present study was carried out in the Moldovita
Basin, along the Dumbravnic Brook. In the section fromthe Dumbravnic Brook, which crosses the Dilma – Deia
and Palamina – Ascutita synclinal structures, the sediments
belong to the Vinetisu Formation. This Formation
represents the last term of the Moldovita lithofacies and it
consists of sandstones and clays, 100 – 120 m thick. The
calcareous sandstones are disposed in beds withthicknesses of 30 – 40 cm (Grasu et al., 2007).
Calcareous nannofossils from the Moldovita Basin,
which constitute the object of our study, have been alreadyinvestigated (Ionesi & Meszaros, 1989), but for anothertime-interval, with respect to the present work. In the
Moldovita Basin, the Oligocene/Miocene boundary wasrecorded in the northern part of the Tarcau Nappe, in the
Vinetisu Formation. Calcareous nannofossils from the
Izvor Brook and from the Jaslo Limestone have been studied. The presence of the NP25 Biozone, with Sphenolithus
ciperoensis, was documented. In the succession from Izvor
Brook that crosses the Dilma – Deia and Palamania – Ascutita synclines, the subsequent biozone is represented by
NN1, with Triquetrorhabdulus carinatus (Ionesi &Meszaros, 1989; Juravle, 2007). Previous studies mainly
focused on the Upper Member of the Jaslo Limestone andon the Vinetisu Formation from the Tarcau Nappe –Moldovita lithofacies. In the Upper Member of the Jaslo
Limestone, an assemblage with S. ciperoensis, typical for
the NP25 Biozone was identified. In the Vinetisu Formation, calcareous nannofossils assemblages studied from thethree members provided the following biozones: the Lower
Member – Sphenolithus ciperoensis Biozone - NP25, andan assemblage with Helicosphaera euphratis, H. recta,
Reticulofenestra bisecta, Pontosphaera enormis (NP25 orNN1); from the Middle Member – NN1 Biozone, with Triquetrorhabdulus carinatus; finally, from the Upper Member, any biozone was identified. Thus, theOligocene/Miocene boundary was evidenced in the terminal part of the Lower Member of the Vinetisu Formation(Ionesi & Meszaros, 1989).
In this work, almost all the calcareous nannofossil taxa
have a wide distribution spanning the Eocene andOligocene in the first part of the section. The most frequent
Paleogene species are basically representative of the

Oligocene: NP21-22 - Reticulofenestra umbilica, Lanternitus minutus, Coccolithus formosus, Cyclicargolithus
floridanus, and NP23-24: Helicosphaera ethologa. In thesecond part of the section, calcareous nannofossil assemblages contain species that are present also at the top of the
Oligocene/Miocene boundary, and are frequent in theLower Miocene: Helicosphaera scissura (NP24-NN4), H.
recta (NP24-NN4), Discoaster deflandrei (NP11-NN7),
Sphenolithus moriformis (NP12-NN9); also Paleogene
species are present. Thus, the presence of the Paleogene/Neogene boundary can be documented in the section
from the Dumbravnic Brook in the Moldovita Basin.
References
Dicea, O. & Dicea, M. 1980. Stratigraphic correlations on nannoplankton basis in the External Flysch of the East Carpathians.
D.S. Inst. Geol. Geofiz., 65: 111-126.
Grasu, C., Miclaus, C., Florea, F. & Saramet, M. 2007. Geologia
si valorificarea economica a rocilor bituminoase din Romania. Ed. Univ. “Alexandru Ioan Cuza”, Iasi: 5-253.
Ionesi, L. & Gheta, N. 1978. Virsta stratelor de Gura Soimului
din semifereastra Humor. Anuarul Muz. de St. Nat. P. Neam,
seria Geologie-Geografie IV.
Ionesi, L. & Meszaros, N. 1989. Sur la limite Oligocene-Miocene
dans le Flysch Externe Carpatique. In: L. Ghergari, N.
Meszaros, E. Nicorici & I. Petrescu (Eds). The Oligocene
from the Transylvanian Basin, Romania. Univ. of Cluj
Napoca, Cluj Napoca: 133-141.
Juravle, D.T. 2007. Geologia regiunii dintre Valea Sucevei si
Valea Putnei (Carpatii Orientali). Casa Editoriala Demiurg,
Iasi: 6-319.
Lebenzon, C. 1973. Nannoplanctonul calcaros al depozitelor
Oligocene si Miocen-inferioare din cursul superior al vaii Tarcaului (valea Tarcuta si valea Rachitis). D.S. Inst. Geol., 59:
101-112.
Martini, E. & Lebenzon, C. 1971. NannoplanktonUntersuchungen im oberen Tal des Tarcau (Ostkarpaten,
Rumaenien) und stratigraphische Ergebnisse. N. Jb. Geol.
Palaeont. Mh., 9: 552-565.
Melinte, M. 1988. Stabilirea limitei Oligocen/Miocen in bazinul
Vaii Buzaului, pe baza nannoplanctonului calcaros. Rom. J.
Stratig., 75(4): 91-97.

Abstracts37

New coccolithophore records from the southern Svalbard
margin: Preliminary results on the SVAIS Cruise sedimentcores
Elena Colmenero-Hidalgo, José-Abel Flores, Francisco J. Sierro, M. Ángeles
Bárcena, Renata G. Lucchi and the SVAIS project participants**Angelo Camerlenghi, David Amblas, Isabel Cacho, Antonio Calafat, Miquel Canals, Jose Luis Casamor,
Sergio Costa, Ben De Mol, Jaume Frigola, Olaia Iglesias, Sara Lafuerza, Galderic Lastras, Caroline Lavoie,
Camino Liquete, Maria Teresa Pedrosa, Roger Urgeles, Joan Grimalt, Andrea Caburlotto, Mauricio Grossi,
Michele Rebesco, Monica Winsborrow

SVAIS is a project supported by the Spanish Government
within the 2007-2009 IPY activities. Its main goal is to contribute to the understanding of the evolution of glacial continental margins and the relationships with the changes in
ice-sheet dynamics induced by climatic changes by: 1) geophysical and stratigraphic high-resolution studies of an icestream-dominated marine depositional system of the Artic
margin, and 2) definition of its sedimentary architectureand seafloor morphology, and record of their evolution
since the onset of glacial conditions. For those reasons, aglacial depositional system on the Southern Svalbard margin (the Storfjiorden margin) was chosen on account of its
relatively small size and its location in a highly climaticallysensitive area near the gateway to the Artic Ocean.
The SVAIS cruise took place in August 2007 onboard
the BIO Hesperides, a Spanish scientific research vessel.
Detailed multibeam bathymetric survey, shallow seismics(TOPAS), single-channel seismic reflection, and coring of
6 sediment cores were performed during the cruise. Two of
the piston cores (SVAIS01 and 04) were recovered in deep
waters in the lower slope, three others (SVAIS02, 03 and05) were sampled in the upper slope, and the last one(SVAIS06, gravity mode) was recovered in the shelf area.
The micropaleontological studies on the SVAIS materials aim to provide a stratigraphic framework for the evolution of the Storfjiorden margin, to obtain apaleoceanographic record that allows the reconstruction of
the margin dynamics in relation to the climatic changes atdifferent temporal scales, and to improve the calibration of
micropaleontological proxies (nannoflora, foraminifers anddiatoms) in the high-latitude sub-arctic region of the Atlantic. The initial micropalentological analysis indicatesthat the recovered sediments are of good quality, with absence of major preservation problems. All cores containmaterial deposited in a time interval that includes the
Holocene and presumably the Deglaciation and some partsof the Last Glacial Period; differentiation between these
periods is made taking into account criteria such as presence/absence of marker species, taxa abundance, diversityof assemblages, and amount of lithics. Holocene sediments
deposited within an oceanographic context similar to thepresent cover the top centimetres of the study area, whilefurther downcore the sedimentation has occurred most
likely in a glacial-like scenario, in which the proximity of
ice-sheets and the extension of sea-ice cover played a majorrole in the oceanographic conditions and deposition
processes, with drastic assemblage changes closely associated with the oscillations in the extent of the nearby seaice.

38

Abstracts

Quantitative analysis of Middle Miocene calcareous
nannofossils from the scientific drilling at Baden-Sooss(Austria, Central Paratethys)
Stjepan Coriç, Johann Hohenegger
Quantitative analyses on calcareous nannofossils were carried out on 102 Middle Miocene samples from the drillingat Baden-Sooss (Vienna Basin) for scientific investigations.
All samples can be assigned to nannoplankton Zone NN5(Martini, 1971). The low concentration of Helicosphaera
walbersdorfensis Müller, 1974 allows correlation with theMediterranean nannoplankton Subzone MNN5a (S. heteromorphus - H. walbersdorfensis Interval Subzone of Fornaciari et al., 1996).
Typical near-shore forms, such as small reticulofenestrids, accompanied by smaller numbers of Umbilicosphaera jafari Müller, 1974, Reticulofenestra haqii
Backman, 1978, Coccolithus pelagicus (Wallich, 1871)
Schiller, 1930, and Reticulofenestra pseudoumbilicus(Gartner, 1967) Gartner, 1969 dominate the calcareous
nannoplankton assemblages. Inter-species correlations andcorrelations to stable isotopes and magnetic susceptibility,
together with multivariate statistical methods (Cluster
analysis, Indicator values method, Nonmetric Multidimensional Scaling) enabled the reconstruction of trends in thepalaeoenvironment of the upper water mass during this partof the Badenian.
The following calcareous nannoplankton species wereanalyzed for palaeoecological interpretation: C. pelagicus,
discoasterids, helicoliths, reticulofenestrids (R. minuta, R.
pseudoumbilicus), sphenoliths (S. heteromorphus, S. moriformis), U. jafarii, and the contribution of reworked nannoplankton from older strata (see figure).
Coccolithus pelagicus is negatively correlated withmagnetic susceptibility, thus higher percentages of thisform coincide with lower values of magnetic susceptibility
and suggest lower water temperature. Vice versa, lower percentages of C. pelagicus can be correlated with peaks ofmagnetic susceptibility. These periods suggest warmer
water due to the higher insolation. Periods of colder, nonstratified water containing higher proportions of C. pelagicus are interpreted in the deeper core between -77 and-71m, then this taxon was replaced in the following interval by stratified, higher-salinity and warmer water. A slight,
but continuous, temperature decrease, starting from -50m
core-depth upwards, resulted in an abundance increase of
C. pelagicus indicating also an eutrophication trend.
Small reticulofenestrids, which occupy marine environments along continental margins, dominate the nannoplankton assemblages in the core. Abundance oscillations
could indicate changes in temperature, inferring warmer,
stratified waters and lower salinity.
Sphenolithids can also be used as temperature indicators. Therefore, higher percentages of Sphenolithus heteromorphus Deflandre, 1953 and S. moriformis(Brönnimann & Stradner, 1960) Bramlette & Wilcoxon,
1967 coincide with increased magnetic susceptibility andcan be used as indicators for increased water temperature.
Umbilicosphaera jafarii is common in shallow environments; the abundance peaks reflect a slight increase insalinity. The transition from a community with abundant
C. pelagicus to U. jafarii needs a slight temperature increase; these transitions are often found in the core. Transitions from communities with abundant U. jafarii tocommunities where R. minuta dominates are discontinuous, needing larger and abrupt environmental changes.
The higher erosion rate on the continent is documented
by high percentages of reworked calcareous nannoplankton. This can be correlated with the intensified input ofmagnetic particles, as documented by magnetic susceptibility.
Low percentages of discoasterids point to a sedimentation environment close to the shoreline.
Low variations in abundance of ecological sensitive
species suggest relatively low fluctuating environments.
The deeper part of the core (-102 to -40m) shows opposite
oscillating trends (with long periods) in salinity and temperature. Around -70m, the salinity maximum is combinedwith a temperature minimum and, vice versa, a salinity
minimum and temperature maximum can be found around-50m. Trends in the upper core are more discontinuous,possibly due to gaps in the sedimentation record as caused
by intensified tectonics. Generally, a linear trend towards
slightly increasing salinity, eutrophication and lowered
temperatures can be documented for the upper core.
This study was financially supported by the Austrian
Science Foundation FWF project P16793-B06.
References
Fornaciari, E., Di Stefano, A., Rio, D. & Negri, A. 1996. Middle
Miocene calcareous nannofossil biostratigraphy in the
Mediterranean region. Micropaleontology, 42(1): 37-63.
Martini, E. 1971. Standard Tertiary and Quaternary calcareous
nannoplankton zonation. Proceedings of the II Planktonic
Conference, Roma, 1971. Ed. Tecnoscienza, Roma: 739-785.

Abstracts

39

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Abstracts

Calcareous nannoplankton composition and flux in responseto the passage of Hurricanes Ignacio and Marty in the SW
Gulf of California
Mara Y. Cortés, Francisco. J. Urcádiz-Cázares, Jörg Bollmann, F. AguirreBahena, Norman Silverberg
Calcareous nannoplankton comprise a group of organismsthat play an important role in the global carbon cycle. Although several studies concerning the vertical flux of coccolithophores to the sediment have been carried out inrecent years, little is known about their distribution and response to short-term events.
As part of a multidisciplinary program, a time-series
sediment trap has been deployed in Cuenca Alfonso, located in Bahía de La Paz, Gulf of California, since January
2002. This area is often influenced by hurricanes duringlate summer – early autumn. This has provided a unique
opportunity to study the seasonal variation of calcareous
nannoplankton and their response to such short-term environmental events.
During 2003, two hurricanes occurred within one
month of each other. Hurricane Ignacio and Hurricane
Marty, followed similar tracks from south to north acrossthe bay, and brought high winds, intense precipitation,
heavy runoff and, for the two weeks including and following the day of each hurricane, high bulk sedimentation rates
were observed (Silverberg et al., 2007). Very high coccolith fluxes were also registered in all 6 samples recovered
during the entire 6-week period. During Hurricane Ignacio, values of 15x108 coccoliths/m2/d were encountered. In
the 2 weeks following the impact of Ignacio, fluxes remained higher than non-hurricane years. Fluxes thenpeaked again, to even higher values (129x108 coccoliths/m2/d), for the 2 weeks following the passage of Marty.
Furthermore, the species composition of the nannoplanktonchanged from a dominance of G. oceanica and E. huxleyi
under normal conditions, to a dominance of F. profunda
during the hurricane-influenced period. Some species encountered rarely or in low abundance during non-hurricane
seasons were more common or abundant during the hurricane period, while some minor species were apparently unaffected.
Reference
Silverberg, N., Shumilin, E., Aguirre-Bahena, F., Rodríguez-Castañeda, A.P. & Sapozhnikov, D. 2007. The impact of hurricanes on sedimenting particulate matter in the semi-arid Bahíade La Paz, Gulf of California. Continental Shelf Research, 27:2513–2522.

Abstracts

Coccolithophore spatial distribution from an extremely
oligotrophic gyre to an intense upwelling in the subtropicalSouth Pacific
Martine J.J. Couapel, Luc Beaufort
Water samples were collected at multiple depths in the euphotic zone on an oceanic transect from the Marquises
Archipelagos to the Chilean upwelling, via the South Pacific Gyre, during the BIOSOPE cruise in austral summer,
2004. Based on full taxonomic identification of the coccolithophore community, we describe the spatial distribution of over 60 species. The coccolith concentration ranges
from 400 to about 360 000 coccospheres/l, while thespecies richness ranges from 7 to 47 species per sample.
The highest species richness is reached at each station
along the transect in the vicinity of the deep chlorophyllmaximum. The highest number of coccospheres and thegreatest species richness are found in the margin of theChilean upwelling system. The low-nutrient, low-chlorophyll South Pacific Gyre, often described as the world’s
poorest desert, is in fact inhabited by a deep coccolithophore community living down to 300 m depth. The
concentration of this community, which is composed of 25
species, reaches about 18 000 coccospheres/l. This is thefirst report of such a deep coccolithophore community
present in an oligotrophic region.
A Principal Component Analysis allowed the definitionof 7 coccolithophore assemblages, each corresponding toan ecological niche. These niches are distributed longitudinally in the upper part of the water column and in depth
in the deepest part of the water column. Assemblage characteristics and distributions can be summarised as follows:
1. in the western part of the transect, in the mesotrophic
area of the Marquise plume, is dominated by Gephyrocapsa spp., Umbellosphaera tenuis and Calcidiscus leptoporus;
2. essentially composed of Umbellosphaera tenuis, Emiliania huxleyi, mini placoliths and Calcidiscus leptoporus corresponds to a high-salinity, high-temperaturearea;
3. found in the oligotrophic area of the South Pacific Gyre,
is characterised by a domination of Syracosphaera spp.
and large coccospheres, such as Rhabdosphaera clavigera and Discosphaera tubifera;
4. mainly composed of placolith bearing coccospheres, ispresent on the outerside of the Chilean upwelling margin and within it;
5. corresponds to the higher-diversity assemblage on theoriental margin of the Chilean upwelling, and below the4 other assemblages, around 150 m depth;
6. spread along the transect in the deeper sampling area,
dominated by Florisphaera profunda, Gladiolithus spp;
7. located in the deeper part of the Chilean upwelling, is
exclusively represented by small-sized placolith bearing coccospheres, and results of the mixing of water

masses.

41

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Abstracts

Ecological implications of the haplo-diploid versatility incoccolithophoresLluïsa Cros, Marta Estrada
Coccolithophores tend to occupy ecological environmentswith an intermediate degree of fertility, midway between
the extremes represented by turbulent, nutrient-rich waters,
which favour diatom growth, and stratified, nutrient-poorwaters, where dinoflagellates and other flagellates dominate (Margalef, 1978).
Studies of the distribution of extant coccolithophores
in well-stratified, summer Mediterranean waters haveshown that the different forms of Helicosphaera carteri inhabit different water depths. The heterococcolith form is
associated with a relatively nutrient-rich DCM (Deep
Chorophyll Maximum) layer, located within the nutricline,
whilst the holococcolith form inhabits the impoverished
upper water levels (Cros, 2001). An interpolation of these
Helicosphaera data, within the conceptual model of Margalef’s Mandala, supports the idea (Houdan et al., 2006)
that the diploid heterococcolithophores and the haploid
holococcolithophores might be exploiting a range oftrophic environmental situations, with ecological niches
closer to those of diatoms for heterococcolithophores andto those of dinoflagellates for holococcolithophores. Thus,
it can be hypothesised that the haplo-diploid versatility of
coccolithophores represents a survival strategy in a changing ecological environment.
References
Cros, L. 2002. Planktonic coccolithophores of the NW Mediterranean. Published PhD thesis. Publicacions de la Universitat
de Barcelona, Barcelona: 365pp.
Houdan, A., Probert, I., Zatylny, C., Véron, B. & Billard, C. 2006.
Ecology of oceanic coccolithophores. I. Nutritional preferences of the two stages in the life cycle of Coccolithus
braarudii and Calcidiscus leptoporus. Aquatic Microbial
Ecology, 44: 291-301.
Margalef, R. 1978. Life-forms of phytoplankton as survival alternatives in an unstable environment. Oceanologica Acta, 1:
493–509.

Abstracts

Volume calculation of Paleocene calcareous nannofossils
Bianca De Bernardi, Claudia Agnini
During the past decades, volume calculation of extant calcareous nannoplankton has been performed in order to convert coccolith fluxe data into carbonate export productivity.
The most useful and relatively recent method to estimate
the volume of coccoliths is described by Young & Ziveri(2000). Several studies on estimates of recent coccolithophore carbonate contribution have been published, andthis methodology has also been successfully applied to
Mesozoic sediments (Tremolada & Young, 2002), thus providing a new, promising proxy to be used in paleoceanographic reconstructions. Based on these fruitful practices,
we have decided to test these methodologies on Paleocene
sediments from several DSDP/ODP sites. The study areas
are located at different latitudes, both in the Atlantic (401,690, 1051, 1260 and 1263) and Pacific (ODP Site 1209)
Oceans, with the intention of giving a global perspective.
We have investigated well-preserved, deep-sea sediments in order to determine the average dimensions, andcalculate the volume of, the most abundant Paleocene nannofossils, which include Coccolithus, Toweius, Sphenolithus, Fasciculithus, Discoaster and Zygrhablithus. For
each taxon, we have measured at least 250 specimens to
obtain accurate size estimates; furthermore, we have analyzed 30 specimens of each species to calculate the shape
constant (Ks), which, in turn, is used to obtain calcareous
nannofossil volumes. This approach permits to evaluate thetotal amount of CaCO3 produced by coccoliths and could
be used to provide an important tool for palaeoecologicaland biogeochemical interpretations. However, the present
work represents the first attempt to investigate the significance of volume variation within Paleocene nannofloras.
References
Tremolada, F. & Young, J.R. 2002. Volume calculation ofCretaceous
calcareous
nannofossils. Journalof
Nannoplankton Research, 24(3): 199-202.
Young, J.R. & Ziveri, P. 2000. Calculation of coccolith volume
and its use in calibration of carbonate flux estimates. DeepSea Research. Part II: Topical Studies in Oceanography, 47:
1679-1700.

43

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Abstracts

Morphologic evolution of Discoaster multiradiatus from theLate Paleocene to the Early Eocene: abiotic and biotic
causesBianca De Bernardi, Elisabetta Erba
A detailed investigation of sediments recovered at ODP
Site 1209 (Shatsky Rise, Pacific Ocean) shows a significant change in Discoaster multiradiatus (incertae sedis)
morphology and size during the Late Paleocene-Early
Eocene. This analysis was extended to selected samples
from other sediment sections at various paleolatitudes andfrom different sedimentary basins to decipher local vs.
global changes.
This time interval is crucial, both for biotic evolution
and environmental changes, being characterized by a series of hyperthermal events. Significant modifications incalcareous phytoplankton morphometry are known in thegeological record but the causes of these size variations arestill under debate. Several authors suggested that size variations could be triggered by paleoceanographic conditions;however, size variability also occurred during times of environmental stability. The goal of the present study is tounderstand if the observed changes in size result from
ephemeral adaptation-malformations or true evolutionarychanges.
For size determination, images of D. multiradiatus werecollected using a digital image-capture system (Young etal., 1996), then an image analyses program (NIH-IMAGE
software) was used in order to document fluctuations intheir maximum diameter. At least 100 specimens were randomly selected through the smear slide of each sample, toprovide accurate size estimate.
Results from morphometric analyses highlight a clear
increase in size through time, overprinted by rapid shifts togigantic forms. The relative timing between climate perturbations and biotic evolution in the Late Paleocene-Early
Eocene, and specifically during the Paleocene/Eocene
Thermal Maximum (PETM) interval, indicates that shortterm size variations and malformations were strongly influenced by environmental pressure. The size variations of
D. multiradiatus suggest that both long-term evolutionary
trends and transient adaptations are somehow controlled byenvironmental pressure.
References
Young, J., Kucera, M. & Chung, H.-W. 1996. Automatedbiometrics on captured light microscope images of Emiliania
huxleyi. In: A. Moguilesky & R. Whatley (Eds). Microfossils
and Oceanic Environments. University of Wales,
Aberystwyth Press: 261-280.

Abstracts

45

Productivity of calcareous nannoplankton duringhyperthermal events: results from Sr/Ca ratios andbiometry
Mascha Dedert, Heather Stoll, Jeremy Young, Patrizia Ziveri
Reconstructing the productivity of calcareous nannoplankton during hyperthermal events can contribute to our understanding of feedbacks to the high atmospheric CO2
concentrations that characterized these events. Increased
primary productivity resulting from increased weatheringand consequently an increased nutrient availability has
been suggested as an important negative feedback (Bains etal., 2000).
The Sr/Ca ratio in coccolith calcite has been shown tobe related to the productivity of calcareous nannoplankton(Stoll & Schrag, 2000; Rickaby et al., 2002). We havemeasured Sr/Ca ratios in monogeneric samples of five different genera, covering the Paleocene Eocene Thermal
Maximum (PETM) and the Early Eocene Hyperthermal
Event (ETM2) Elmo, in order to reconstruct the productivity response of calcareous nannoplankton to these
events. Nannofossils were isolated from ODP Cores 1263C
and 1265A, located on the Walvis Ridge, using the method
described by Stoll et al. (2007).
During the PETM, the Sr/Ca ratios in both C. pelagicus
and Toweius increased, suggesting a high nutrient availability. Initial Sr/Ca ratio measurements in individual discoasters and Zygrhablithus bijugatus revealed a different
ecological response, with Discoaster increasing in productivity at the onset of the PETM, followed by an increase inproductivity of Zygrhablithus. The cold-water taxon Chiasmolithus did not show a response to the event, except fora small increase in productivity at the onset of the PETM.
We will compare the PETM Sr/Ca record with the
Sr/Ca and oxygen isotope record covering the Early Eocene
Hyperthermal Event (ETM2) Elmo at ODP Site 1265,
which is closely located to Site 1263. The oxygen isotopes
were measured in size fractions that are dominated bypelagic nannofossil carbonate. The warming trend foundin the O-isotope signal coincides with the increase in Sr/Ca
ratios in two dominating genera, C. pelagicus and Toweius.
Biometric analyses of C. pelagicus and Toweius demonstrate an increase in average coccolith size. These increases
correlate with the Sr/Ca productivity and O-isotope warming signal, and could indicate an ecological response.
References
Bains, S., Norris, R.D., Corfield, R.M. & Faul, K.L. 2000. Termination of global warmth at the Paleocene/Eocene boundary
through productivity feedback. Nature, 407: 171-174.
Rickaby, R.E.M., Schrag, D.P., Zondervan, I. & Riebesell, U.
2002. Growth rate dependence of Sr incorporation during calcification of Emiliania huxleyi. Glob. Biogeochem. Cycles,
16(1).
Stoll, H.M. & Schrag, D.P. 2000. Coccolith Sr/Ca as a new indicator of coccolithophorid calcification and growth rate. Geo-chemistry, Geophysics and Geosystems, 1: 1999GC000015.
Stoll, H.M., Shimizu, N., Arevalos, A., Matell, N., Banasiak, A.
& Zeren, S. 2007. Insights on coccolith chemistry from a newion probe method for analysis of individually picked coccoliths. Geochemistry, Geophysics and Geosystems, 8: Q06020,
doi: 10.1029/2006GC001546.

46

Abstracts

Overgrowth on Discoaster and Zygrhablithus during the
PETM: results from Sr/Ca measurements, stable isotopes
and SEM analyses
Mascha Dedert, Heather Stoll, Jeremy Young, Patrizia Ziveri
Discoasters are useful biostratigraphic markers. Their origin, however, is still under debate. SEM analysis revealed
that discoasters and Zygrhablithus, present in sediments
covering the Late Paleocene to Early Eocene, are severely
overgrown. This overgrowth was demonstrated geochemically by measuring Sr/Ca ratios in individual specimensof Discoaster covering the Early Eocene Hyperthermal
Event (ETM2) Elmo. Also, stable isotope results obtained
from separated size fractions that are dominated by discoasters indicate that calcification either took place deepin the water column, which would be in agreement with thegeneral assumption that discoasters are deep-dwellers, or
could be interpreted as discoasters being largely composedof carbonate that was formed during early diagenesis.
As a means of demonstrating the overgrowth on bothnannolith taxa, we present overgrowth profiles of Discoaster and Zygrhablithus during the Paleocene Eocene
Thermal Maximum (PETM), ODP Core 1263C, Walvis
Ridge. The overgrowth profiles were obtained during
measurements of Sr/Ca ratios through individual Discoaster and Zygrhablithus with an ion probe. The amountof overgrowth was calculated by comparing the primarycalcite Sr/Ca with the Sr/Ca measured in the Discoastersize fractions. Overgrowth profiles and SEM images imply
that the secondary calcite covering the nannoliths is dissolved during deep-sea carbonate dissolution that accompanied the PETM or was never formed.
Furthermore, we analysed the overgrowth on these two
nannolith species throughout the PETM interval at different sites. The degree of overgrowth varied throughout theinterval and at different sites, and correlates to geochemical conditions in the sediment.

Abstracts

Middle Miocene lineages in the calcareous nannofossil
genus Discoaster
Eric de Kaenel, James Bergen
Research was conducted on the entire Miocene composite
section from ODP Leg 154 (Ceara Rise, Western Equatorial Atlantic) between 2001 and 2008. The main purpose
was to calibrate the latest cyclostratigraphic-based timescale to the nannofossil biostratigraphic framework in the
deep-water Gulf of Mexico. Routine sampling was done at
20 kyr intervals, with some intervals sampled at 10 kyr resolution.
Middle Miocene lineages for discoasters with large central areas are presented, including four species described
between 1954 and 1981: Discoaster deflandrei, Discoastermusicus, Discoaster kugleri and Discoaster sanmiguelensis. Eight new species within these lineages are proposed toaccount for variations in morphology with demonstrated
stratigraphic utility. The main variations in morphology
used to delineate these forms with large central areas are:1) central area periphery (rounded or hexagonal);
2) distal central area (presence/absence of a knob);3) proximal central area (presence/absence of knobs andridges)4) ray dimensions (length and width);5) ray outline (tapered, parallel-sided, flared);6) ray terminations (bifurcated, rounded, pointed, indented,
notched).
These species normally range between 8-15 microns,
but very rare specimens less than 8 microns also occur.
Comparisons, including schematic drawings and light micrographs, are presented to differentiate four different lineages and their associated species. Their stratigraphy isthen presented relative to defined middle Miocene zones.
The total range of Discoaster sanmiguelensis and its variants is lowermost NN4 (17.69 Ma) to uppermost NN8(11.04 Ma). The Discoaster musicus group ranges from theupper NN5 to the upper NN6 (13.08 Ma). Discoaster kugleri variants clearly predate (12.97 Ma) the base of Zone
NN7 (11.910 Ma), as defined in both the NN and CN zonal
schemes, by the first occurrence of Discoaster kugleri.

47

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Abstracts

New tools for detecting the Miocene/Pliocene boundary in
the Mediterranean region by means of calcareous
nannofossils
Agata Di Stefano, Gioconda Sturiale
The recognition of the Miocene/Pliocene boundary in the
Mediterranean region by means of calcareous nannofossil
has been widely debated. Three important biological eventstake place very close to the Zanclean base and are very wellconstrained outside the Mediterranean: the last occurrence(LO) of Triquetrorhabdulus rugosus, the first occurrence(FO) of Ceratholithus acutus and the LO of Discoaster
quinqueramus, respectively astronomically calibrated at5.231 Ma, 5.372 Ma and 5.537 Ma by Backman & Raffi(1997). All these biohorizons anyway show low applicability in the Mediterranean region. The presence of typical
Discoaster quinqueramus is a controversial point. Many
authors (e.g. Raffi et al., 2003 and reference therein) assess that this species, and the co-distributed, similar D.
bergrenii, are not present in the Mediterranean area. On theother hand, the presence of typical specimens is documented in the Mediterranean area (Mazzei, 1985; Cipollari& Cosentino, 1995; Iaccarino et al., in press), but the scattered distribution and the low frequencies do not allow todefine either a FO or a LO at synchronous levels in the
Mediterranean area.
Both T. rugosus and C. acutus are rare in the Mediterranean area. Rio et al. (1984) and Di Stefano et al. (1996)
did not mention the presence of C. acutus in the Zancleanof the Capo Rossello area and southern Italy. Castradori(1998) points out the presence of very rare C. acutus only
in one sample in the basal Zanclean sediment of Site 969B
succession (Eastern Mediterranean).
Here, we present data from four sedimentary sequences
encompassing the Miocene/Pliocene boundary, located indifferent areas of the Mediterranean basin. From west toeast, we have selected ODP Hole 975B (Balearic Basin,
western Mediterranean), the Cava Serredi section (Tuscany,
central Italy), the Montepetra borehole (Emilian Apennines, NE Italy) and ODP Hole 969B (Mediterranean
Ridge, eastern Mediterranean). All the selected sections
have been investigated at high resolution, with the exception of the Montepetra borehole, performing quantitative
analyses on the whole assemblage, to better highlight thepresence of useful biohorizons.
Our study confirms that C. acutus and T. rugosus arevery rare in the Mediterranean area, and do not provide useful bioevents through the investigated sections. Particularattention has been payed to selected taxa that were known
to be potentially useful for biostratigraphy. The quantitative analyses on the Reticulofenestra genus pointed out thepresence of a sharp paracme interval, very close to the Zanclean base, previously documented on a qualitative basis(Castradori, 1998; Di Stefano et al., 1996). On the contrary,small reticulofenestrids (less than 7 μm) dominates the nan-nofossil assemblage within the same stratigraphic interval.
In addition, we have tested the biostratigraphic value of apeculiar circular morphotype of Reticulofenestra, whose
presence seems to be restricted to the lowermost part of theZanclean.
References
Backman, J. & Raffi, I. 1997. Calibration of Miocene nannofossil events to orbitally tuned cyclostratigraphies from Ceara
Rise. In: N.J. Shackleton et al. (Eds). Proc. ODP, Sci. Res.,
154: 83-99.
Castradori, D. 1998. Calcareous nannofossils in the basal Zanclean of the Eastern Mediterranean Sea: remarks on paleoceanography and sapropel formation. In: A.H.F. Robertson etal. (Eds). Proc. ODP, Sci. Res., 160: 113-123.
Cipollari, P. & Cosentino, D. 1995. Miocene unconformities in
the central Apennines: geodynamic significance and sedimentary basin. Tectonophysics, 252: 375-389.
Di Stefano, E., Sprovieri, R. & Scarantino, S. 1996. Chronologyof biostratigraphic events at the base of the Pliocene. Paleopelagos, 6: 401-414.
Iaccarino, S.M., Bertini, A., Di Stefano, A., Ferraro, L., Gennari,R., Grossi, F., Lirer, F., Manzi, V., Menichetti, E., Ricci
Lucchi, M., Taviani, M., Sturiale, G. & Angeletti, L. 2008.
The Trave section (Monte dei Corvi, Ancona, Central Italy):an integrated paleontological study of the Messinian
deposits. Stratigraphy, in press.
Mazzei, R. 1985. The Miocene sequence of the Maltese Islands:
biostratigraphic and chronostratigraphic reference based onnannofossils. Atti della Società Toscana di Scienze Naturali,
Serie A, 92: 165-197.
Raffi, I., Mozzato, C., Fornaciari, E., Hilgen, F.J. & Rio, D. 2003.
Late Miocene calcareous nannofossil biostratigraphy and astrochronology for the Mediterranean region. Micropaleontology, 49: 1-26.
Rio, D., Sprovieri, R. & Raffi, I. 1984. Calcareous plankton biostratigraphy and biochronology of the Pliocene-lower Pleistocene succession of the Capo Rossello area, Sicily. Mar.
Micropaleontol., 9: 135-180.

Abstracts

New perspectives on the Cenozoic history of the
Syracosphaerales
Tom Dunkley Jones, Paul Bown, Jeremy Young
The Order Syracosphaerales includes the two most diverse
modern coccolithophore families, the Syracosphaeraceae
and Rhabdosphaeraceae, and forms approximately half ofmodern heterococcolithophore biodiversity. An understanding of its evolutionary history has, however, beenhampered by the relatively poor fossil record of the often
small and fragile coccoliths produced by these taxa, and bysome dubious assignments of taxa to the modern genera.
Recently acquired palaeontological data from locations
with exquisite nannofossil preservation (Tanzania, New
Zealand, US Gulf Coast and Para-Tethys) provide newmorphological and taxonomic data, constraints on origination times for major extant genera, and an outline of longterm patterns of diversity through the Cenozoic.
The pattern of Rhabdosphaeraceae diversification in theearly Eocene, with peak diversities in the middle Eocene,
before a long-term decline through the late Eocene andearly Oligocene, is supported, but new, deep-time occurrences of the extant genera Acanthoica (late Paleocene),
Rhabdosphaera (middle Eocene) and Algirosphaera (late
Eocene) are documented for the first time, together withexceptional morphological and species diversities in the
Eocene genus Blackites.
The Syracosphaeraceae are present in the fossil record
by at least the late Paleocene, but remain at relatively low(preserved) diversities and with conservative morphologies
through the Eocene, Oligocene and Miocene in contrast to
their high diversity in the modern oceans. Available molecular genetic data indicate a late Mesozoic divergencetime for the Syracosphaeraceae, and the relationship between the Cenozoic families and the Mesozoic to modern
Calciosoleniaceae will be discussed.

49

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Abstracts

Dwarf coccoliths at the onset of Cretaceous Oceanic Anoxic
Events 1a and 2: an example of calcareous nannoplankton
sensitivity to excess CO2?
Elisabetta Erba, Cinzia Bottini
High-resolution sampling of the initial phase of both early
Aptian Oceanic Anoxic Event (OAE) 1a and latest Cenomanian OAE 2 was applied to relatively expanded sections
from the western Tethys. Quantitative and morphometricinvestigations of calcareous nannofossil assemblages
pointed out the occurrence of dwarf coccoliths. Small specimens of genera Biscutum, Zeugrhabdotus and Discorhabdus become relatively common, and parallel the decrease inabundance of large nannofossils, such as the heavily calcified nannoconids and other nannoliths.
During the mid-Cretaceous, the natural source of atmospheric CO2 was Earth’s degassing, and emplacementof the Ontong Java-Manihiki and Caribbean Plateau large
igneous provinces (LIPs) is recognized as responsible for
pCO2 as high as 2000 ppm. Coeval (and synchronous) biocalcification crises have been documented in pelagic andneritic settings, suggesting a causal link between high concentrations of carbon dioxide in the atmosphere-ocean system and drops in benthic and planktonic calcifiers’
efficiency.
Coccolith dwarfism is here interpreted as forced by rapidly increasing pCO2, and might be the counterpart of the
major decrease in nannolith abundance. Our data are consistent with works by Riebesell et al. (2000), but are apparently contradicted by recent data by Iglesias-Rodriguez
et al. (2008), documenting enlarged Emiliania huxleyi coccoliths under high CO2.
We stress the fact that: (1) coccolith size alone is not ameasure of calcite production (number of coccoliths must
be taken into account) and of calcification rate; (2) E. huxleyi is not the best taxon for testing biocalcification: thisspecies is super-opportunistic and might take advantage inany environment; (3) during OAEs pCO2 concentrations
were so elevated as to exceed threshold values, and current
lab experiments might not be good analogues.
Although dwarf coccoliths might result from enhanced
fertility associated with OAE1a and OAE2, regardless ofocean alkalinity, all geological data indicate a rapid, 4 to
10 times increase of pCO2 associated with both episodesof global anoxia. We believe that the observed tiny specimens derive from difficult/reduced calcification and suspect that in order to reproduce and understand rates ofCretaceous nannoplankton mineralization, future lab experiments should be run under pCO2 as high as 1500-2000
ppm.
References
Iglesias-Rodriguez, D., Halloran, P.R., Rickaby, R.E.M., Hall,
I.R., Colmenero-Hidalgo, E., Gittins, J.R., Green, D.R.H.,
Tyrrell, T., Gibbs, S.J., von Dassow, P., Rehm, E., Armbrust,
E.V. & Boessenkool, K.P. 2008. Phytoplankton Calcification

in a High-CO2 World. Science, 320: 336-340.
Riebesell, U., Zondervan, I., Rost, B., Tortell, P.D., Zeebe, R.E. &Morel, F.M.M. 2000. Reduced calcification of marine
plankton in response to increased atmospheric CO2. Nature,
407: 364-367.

Abstracts

51

Calcareous nannofossils of the Turonian-Santonian
sediments, Zagros Basin, Iran
Fereshte Farhad, Anoshiravan L. Kani
Due to the lack of any precise paleontological study, thesediments of the Surgah Formation from two well sectionsin the Tange Bijar Gas Field (Sites 7 and 10; see figure)were investigated for their calcareous nannoplankton content to obtain their exact age. Lithostratigraphically, theSurgah Formation consists of an alternating sequence ofmarls and shales with argillaceous limestone intercalations.
Forty samples from Site 7 (with a sample spacing of 5 meters) and seventy samples from Site 10 (with a sample spacing of 2 meters) were collected, prepared and studied under
the light microscope. These samples yielded a rich nannofloral assemblage of 56 species and 31 genera. The distribution of the nannofossil taxa reveals the presence ofUC8-UC12 zones of Burnett (1998) equivalent to CC13CC15 zones of Sissingh (1977), thus pointing to an early
Late Turonian – Early Santonian age for the sediments.
Based on the obtained data, the environmental conditionsof the sedimentary basin of the Surgah Formation is presumed to correspond to a low-latitude, shallow sea, withwarm surface waters rich in nutrients.

References
Burnett, J.A. 1998. Upper Cretaceous. In: P.R. Bown (Ed.). Calcareous Nannofossil Biostratigraphy. Chapman &Hall/Kluwer Academic Publishing, London: 132-200.
Sissingh, W. 1977. Biostratigraphy of Cretaceous calcareous
nannoplankton. Geol. Mijnbouw, 56: 37-65.

52

Abstracts

High-resolution calcareous nannofossil biostratigraphy andchemostratigraphy of the Cenomanian-Turonian boundary
in the Vocontian Basin, south-east France
Allan Gil S. Fernando, Reishi Takashima, Hiroshi Nishi, Hisatake Okada
The Cenomanian-Turonian boundary (CTB) Oceanic
Anoxic Event 2 (OAE2) is considered the type example ofthe Mesozoic OAEs, associated with a large and abrupt perturbation in atmospheric pCO2, changes/turnover in the marine macro- and microfauna, changes in ocean waterchemistry, and a pronounced positive excursion in the δ13C
record of the marine carbonate and marine and terrestrialorganic matter. The positive shift in the δ13C curve is believed to be related to the widespread burial of isotopicallylight organic matter, in response to enhanced oceanic productivity during a period of large igneous province (LIP)
formation (i.e., Caribbean Plateau) and increased submarine volcanism, ocean crust production and hydrothermal
activity, as substantiated by available strontium (87Sr/86Sr)
isotope and trace metal distribution data.
The Thomel Level of the Lambruisse section in the Vocontian Basin in south-east France accumulated during the
CTB OAE2, and is marked by intercalations of black shale
and organic-rich marl. Biostratigraphic analysis of the section revealed a total of 6 nannofossil zones, corresponding
to the UC2-UC9 zones (Lower Cenomanian-Middle Turonian). The result correlates well with the previously established planktonic foraminiferal biostratigraphy in thesection. Biostratigraphically important taxa observed in thesection include Cretarhabdus striatus, Axopodorhabdus albianus, Lithraphidites acutus, Corollithion kennedyi, Helenea chiastia, Quadrum gartneri, Q. intermedium,
Eiffellithus eximius, Eprolithus octopetalus and E. eptapetalus. Helenea chiastia and Q. gartneri, the two nannofossil taxa commonly used in the delineation of the C-Tboundary (e.g., Sissingh, 1977; Perch-Nielsen, 1985;
Bralower, 1988; Bralower et al., 1995; Burnett, 1998; Luciani & Cobianchi, 1999; Paul et al., 1999; Tsikos et al.,2004), occur less than 2m apart in the studied section,
within the UC6 and the Whiteinella archaeocretacea zones.
Detailed litho- and chemostratigraphic analyses indicatethat the δ13C profile of the section corresponds well withchanges in lithofacies and fluctuations in the total organiccarbon (TOC) and calcium carbonate content of the section. Initial increase in the δ13C values occurs within the
UC3-UC4a composite zone, coinciding with the onset ofthe deposition of the organic-rich sediments of the Thomel
Level and drastic decline in the CaCO3 values. The plateau
of high δ13C values, on the other hand, occurs within the
UC5 zone, between the LO of C. kennedyi and the LO of
H. chiastia. This interval of high δ13C values also corresponds to the interval of high TOC and low CaCO3 values.
During the biostratigraphic investigation of the Lambruisse section, the common occurrence of large specimens(>8 μm) of Assipetra terebrodentarius (i.e., A. terebroden-

tarius youngii) was observed in the black shales of theThomel Level, within the UC3-UC5 nannofossil zones.
The increase in abundance and size of this nannolith iswell-documented in the Early Aptian OAE1a (e.g., Erba,
1994, 2004; Tremolada & Erba, 2002), but these trends
have never been documented in younger OAEs, particularly OAE2. Although the paleoecology of Assipetra is still
poorly understood, the taxon’s presence in OAE1a and
OAE2 (both considered as high productivity events or POAEs; Erbacher et al., 1996) suggests possible affinity forhigher fertility of surface waters and, therefore, supports
its potential as a high-productivity indicator-taxon, as suggested by earlier studies (e.g., Tremolada & Erba, 2002).
One new holococcolith taxon, a species of Owenia, is described in this study.
References
Bralower, T.J. 1988. Calcareous nannofossil biostratigraphy andassemblages of the Cenomanian-Turonian boundary interval:
implications for the origin and timing of oceanic anoxia. Paleoceanography, 3: 275-316.
Bralower, T.J., Leckie, R.M., Sliter, W.V. & Thierstein, H.R.
1995. An Integrated Cretaceous Microfossil Biostratigraphy.
In: W.A. Berggren, D.V. Kent, M.-P. Aubry & J. Hardenbol(Eds). Geochronology, Time Scales and Global Stratigraphic
Correlation. SEPM Special Publication, No.54: 65-79.
Burnett, J.A. 1998. Upper Cretaceous. In: P.R. Bown (Ed.). Calcareous Nannofossil Biostratigraphy. British Micropalaeontological Society Publications Series, Chapman &Hall/Kluwer Academic Publishers: 132-199.
Erba, E. 1994. Nannofossils and superplumes: The early Aptian“nannoconid crisis”. Paleoceanography, 9(3): 483-501.
Erba, E. 2004. Calcareous nannofossils and Mesozoic anoxic
events. Marine Micropaleontology, 52(1-4): 85-106.
Erbacher, J., Thurow, J. & Littke, R. 1996. Evolution patterns ofradiolaria and organic matter variations: A new approach toidentify sea-level changes in mid-Cretaceous pelagic environments. Geology, 24(6): 499-502.
Luciani, V. & Cobianchi, M. 1999. The Bonarelli Level and otherblack shales in the Cenomanian-Turonian of the northeastern
Dolomites (Italy): calcareous nannofossil and foraminiferal
data. Cretaceous Research, 20: 135-167.
Paul, C.R.C., Lamolda, M.A., Mitchell, S.F., Vaziri, M.R., Gorostidi, A. & Marshall, J.D. 1999. The Cenomanian-Turonianboundary at Eastbourne (Sussex, UK): a proposed European
reference section. Palaeogeography, Palaeoclimatology,
Palaeoecology, 150: 83-121.
Perch-Nielsen, K. 1985. Mesozoic calcareous nannofossils. In:
H.M. Bolli, J.B. Saunders & K. Perch-Nielsen (Eds). Plankton Stratigraphy. Cambridge University Press: 17-86.
Sissingh, W. 1977. Biostratigraphy of Cretaceous calcareous
nannoplankton. Geologie en Mijnbouw, 56: 37-65.
Tremolada, F. & Erba, E. 2002. Morphometric analyses of Aptian
Assipetra infracretacea and Rucinolithus terebrodentarius

Abstracts
nannoliths: implications for taxonomy, biostratigraphy andpaleoceanography. Marine Micropaleontology, 44: 77-92.
Tsikos, H., Jenkyns, H.C., Walsworth-Bell, B., Petrizzo, M.R.,
Erba, E. Premoli Silva, I., Forster, A., Kolonic, S., Wagner,
T. & Sinninghe Damste, J.S. 2004. Carbon isotope stratigraphy recorded by the Cenomanian/Turonian Oceanic Anoxic
Event: Correlation and implications based on three key-localities. Journal of the Geological Society of London, 161(4):711-719.

53

54

Abstracts

Distribution of ‘minor’ calcareous nannofossil species in thesurface sediments along the Vietnam upwelling zone:
western South China Sea revisited
Adrian Raymund C. Fernandez, Allan Gil S. Fernando
The South China Sea has been studied for calcareous nannofossils (and nannoplankton) since the 1970s and, thus,
has a well established database regarding nannofossil distribution. Similar to other marginal basins, however, the assemblage is dominated by a very few number of taxa,
particularly Emiliania huxleyi, Florisphaera profunda andGephyrocapsa oceanica. Minor species (i.e., species with
abundance values <3% and percent occurrence <70%)comprise <28% of total assemblages (Fernando et al.,2007). Although some of these minor species show possible affinities for particular oceanographic conditions, theinitial data is insufficient to clearly establish their environmental preference due to the overwhelming dominance of
E. huxleyi, F. profunda and G. oceanica. Examples include
Reticulofenestra spp., Calciosolenia murrayi, Helicosphaera carteri and Syracosphaera spp. for neritic conditions, G. ericsonii for low sea-surface temperature
conditions (SSTs) and C. murrayi and Syracosphaera spp.
for warmer SSTs (Fernando et al., 2007). To validate andconfirm these observations, a separate count exclusive ofthe three major taxa will be done and subjected to multivariate analysis, along with several oceanographic parameters, including salinity, whose relationship with somespecies in the South China Sea (e.g., G. ericsonii, Calcidiscus leptoporus, C. murrayi and Syracosphaera spp.)
remains uncertain.
Reference
Fernando, A.G.S., Peleo-Alampay, A.M. & Wiesner, M.G. 2007.
Calcareous nannofossils in surface sediments of the eastern
and western South China Sea. Marine Micropaleontology, 66:
1-26.

Abstracts

55

Geochemical and isotopic signals (Sr/Ca ratios, stable δ13C
and δ18O isotopes) in coccolith carbonate of different grainsize fractions in Atlantic sediments
Christina Fink, Karl-Heinz Baumann
Coccolithophores are unicellular, marine algae and therefore directly dependent on the surface-water conditions inworld oceans. They are one of the main open ocean primary producers and one of the dominant carbonate contributors to pelagic sediments (Westbroek et al., 1993).
Therefore, these organisms influence the chemical composition of surface water by their calcification and photosynthetic mechanisms in different ways. As photosyntheticorganisms, their chemistry and stable isotope composition
can provide a sensitive tool for understanding photic zone
processes (Honjo, 1976). The chemistry of coccoliths
serves both as a record of changes in the chemistry of theocean, and a record of environmental and biological conditions like temperature and productivity (Stoll & Ziveri,2004). Nevertheless, their effect on, and response to, theclimate system is one of the big questions facing our field
today, since coccolith geochemistry has hardly been explored.
The studied surface sediment samples from the equatorial to South Atlantic show that the geochemistry and isotopic composition of coccoliths is dependent on coccolith
growth rate and environmental influences, such as temperature and nutrient supply. The investigations also indicate
a great variability between the different grain size fractions.
Even if the absolute values show a great difference, thegeneral trends are similar: the δ18O ratios in these samples
show a decreasing trend with increasing temperature, while
δ13C and Sr/Ca ratios are influenced by a mixture ofprocesses, such as temperature, nutrient- and probably
freshwater supply. The knowledge of geochemical and isotopic behaviour of coccoliths is used to reconstruct longterm-changes in paleoceanography and paleoclimate. The
coccolith assemblages in ODP Site 659, from the eastern
north-eastern Atlantic, show a distinct shift at the PlioPleistocene boundary. The reticulofenestrids, which arevery abundant in the Pliocene, are replaced by gephyrocapsids in Pleistocene times (Su, 1996). The variation inaccumulation rates of coccolith species and variation inbenthic δ18O values have shown climatic instability during
the late Pliocene and Pleistocene, where low coccolith fluctuation rates are often parallel to low δ18O values (Su,1996). To examine the main influences that caused the shift
in faunal association, the geochemical and isotopic parameters in monospecific coccolith carbonate will be measured.
References
Honjo, S. 1976. Coccoliths: Production, transportation and sedimentation. Marine Micropaleontology, 1: 65-79
Stoll, H.M. & Ziveri, P. 2004. Coccolithophorid-based geochemical paleoproxies. In: H.R. Thierstein & J. Young (Eds). Coc-colithophores - from molecular processes to global impact.
Springer, Berlin: 529-562.
Su, X. 1996. Development of late Tertiary and Quaternary coccolith assemblages in the Northeast Atlantic. Glomar Report,
48: 1-119.
Westbroek, P., Brown, C.W., Bleijswijk, J.v., Brownlee, C., Brummer, G.J., Conte, M., Egge, J., Fernandez, E., Jordan, R.,
Knappertsbusch, M., Stefels, J., Veldhuis, M., van der Wal, P.
& Young, J. 1993. A model system approach to biological climate forcing. The example of Emiliania huxleyi. Global andPlanetary Change, 8(1-2): 27-46.

56

Abstracts

High-resolution Late Eocene-Late Oligocene
biostratigraphy from Site 1090 (Agulhas Ridge, South
Atlantic)
Chiara Fioroni, Davide Persico, Laura Pea, Silvia Palandri, Giuliana Villa
Results are presented of a quantitative biostratigraphic
study of the calcareous nannofossils from the ODP Site
1090 Hole B. It is located in the central part of the Subantarctic Zone on the southern flank of the Agulhas Ridgein the Atlantic sector of the Southern Ocean, above the calcium-carbonate compensation depth (CCD). The base of
the section is composed of late Eocene nannofossil oozes
mixed with red clays deposited at low sedimentation rates
overlain by an extended succession of biosiliceous oozes
and muds, comprising most of the late Eocene, and the late
Oligocene.
Site 1090 proved to be a suitable section for high-resolution biostratigraphic studies (Marino and Flores, 2002).
Part of their nannofossil biostratigraphy was reexaminedusing closely spaced samples and new data are presented
here for the Late Oligocene. For this Site, also a detailed
planktonic foraminiferal biostratigraphy (Galeotti et al.,2002), a robust magnetostratigraphy (Channell et al, 2003)
and a late Oligocene astronomical calibration (Billups etal., 2004) are available. Age estimates for the nannofossil
biohorizons recognized in the section were obtained
through direct correlation to the magnetostratigraphy.
Although nannofossils are at times scarce, some intervals are barren, and preservation varies from good to very
poor, it has been possible to precisely define most of thebiostratigraphic events of the Martini (1971) and Okada
and Bukry (1980) schemes. Nevertheless being Sphenoliths rare at these southern latitudes, it was difficult to recognize the Oligocene standard biozones, therefore
additional bioevents have been proposed. This study allows
the comparison and the improvement of the Paleogene calcareous nannofossil Zonal Scheme for the Southern Ocean.
Part of the scheme has been previously proposed for the
Middle Eocene-Late Oligocene interval (Wei and Wise,
1992; Villa et al., submitted).
We compared our biochronology with data available
from other Southern Ocean sections (748, 689, 744, 738),
confirming the diachronous character of some bioeventsand highlighting in particular how the modified climaticconditions affected nannofossil assemblages of different
latitudes.
Additionally, nannofossil total abundances, relative
abundance of dominant species, and species group abundances were determined to evaluate the potential of thissection for obtaining palaeoecological information.
References
Billups, K., Palike, H., Channell, J.E.T, Zachos, J.C. & Shackleton, N.J. 2004. Astronomic calibration of the late Oligocene
through early Miocene geomagnetic polarity time scale. Earth
Planetary Science Letters, 224: 33-44.

Channell, J.E.T., Galeotti, S., Martin, E.E., Billups, K., Scher, H.
& Stoner, J.S. 2003. Eocene to Miocene magnetostratigraphy,
biostratigraphy, and chemostratigraphy at ODP Site 1090
(sub-Antarctic South Atlantic). Geological Society of America Bulletin, 115: 607-623.
Galeotti, S., Coccioni, R. & Gersonde, R. 2002. Middle Eocene– Early Pliocene Subantarctic planktic foraminiferal biostratigraphy of Site 1090, Agulhas Ridge. Marine Micropaleontology, 45: 357-381.
Marino, M. & Flores, J.-A. 2002. Middle Eocene to Early
Oligocene calcareous nannofossil stratigraphy at Leg 177 Site
1090. Marine Micropaleontology, 45: 383-398.
Martini, E. 1971. Standard Tertiary and Quaternary calcareous
nannoplankton zonation. In: A. Farinacci (Eds). Proceedings
2nd Int. Conf. Planktonic Microfossils, Roma, 2: 739-785.
Okada, H. & Bukry, D. 1980. Supplementary modification andintroduction of code numbers to the low latitude coccolith
biostratigraphic zonation (Bukry 1973, 1975). Marine Micropaleontology, 5: 321-325.
Villa, G., Fioroni, C., Pea, L., Bohaty, S. & Persico, D. Submitted. Middle Eocene – Late Oligocene climate variability: calcareous nannofossil response at Kerguelen Plateau, Site 748.
Marine Micropaleontology.
Wei, W. & Wise, S.W., Jr. 1990. Middle Eocene to Pleistocene
calcareous nannofossils recovered by Ocean Drilling Program
Leg 113 from the Weddell Sea. In: P.F. Barker, J.P. Kennet etal. Proceedings ODP, Scientific Results, 113: 639-666.

Abstracts

57

Coccolithophore response to abrupt and short-term climatechanges in the Gulf of Lions (western Mediterranean) forthe last 25 000 years
José-Abel Flores, Francisco J. Sierro, Elena Colmenero-Hidalgo, José M.
Gravalosa, Miquel Canals, Jaume Frigola, Joan O. Grimalt, Serge Berné,
Bernard Dennielou
Cores PRGL-1 (310 m long) and MD99-2348 (21.5 mlong) were recovered in the Gulf of Lions (42.690N;
03.838 E) at 298.48 m water depth, during the PROMESS
1 (SRV Bavenit drilling vessel) and IMAGES V (RV Marion Dufresne, Calypso piston core) cruises, respectively.
The high sedimentation rates, estimated by robust 14C dating, have given us an excellent opportunity to perform
high-resolution analyses on these materials.
In this study, we present data from the last 25 kyr. The
retrieved sediments consist of silty-clay terrigenous material mixed with small amounts of calcareous microfossils.
Quantitative analyses of coccolithophore assemblages
allow us to identify significant changes in sea-surface temperatures (SST) in this period. Cold peaks are marked byincreases in the proportion of Gephyrocapsa muellerae andlarge morphotypes of Emiliania huxleyi (>5 μm); some of
the most significant can be correlated with Heinrich events.
The high sedimentation rates observed during most of thestudied interval also allow us to identify an overprinted
multicentennial-scale pattern related to DansgaardOeschger cycles. The combined analyses of coccolithophores and planktonic foraminifers permit to produce a
SST record in which sharp fluctuations of around 4˚C inamplitude have been detected. These abrupt changes in
SST are also linked to changes in surface productivity andin the deep and intermediate water dynamics, probably related to variations in the atmospheric patterns (NAO-likeoscillations).
PROMESS 1 is funded by the European Community(EVR1-T-40024).

58

Abstracts

Biostratigraphy of late Sinemurian-Pliensbachiancalcareous nannofossils in northern Spain (BasqueCantabrian Basin)Ángela Fraguas, Nicola Perilli, María José Comas-Rengifo
The aim of this work is to improve the knowledge of nannofossil biohorizons in the Basque-Cantabrian Basin(BCB), through comparison of our results to the scheme
proposed by Bown & Cooper (1998) for NW Europe. The
four ammonite-controlled successions we studied consistof Upper Sinemurian (Raricostatum Ammonite Zone) limestones of shallow platform, grading to a regular alternationof hemipelagic marlstones and limestones, Pliensbachianin age. Our results are based on semiquantitative analysis
of more than 140 smear slides from the Tudanca and Santotis sections, and the re-analysis of more than 200 samples from the Camino and San Andrés sections (Perilli &Comas-Rengifo, 2002).
In the BCB, the most relevant composition changes inPliensbachian calcareous nannofossil assemblages are thefirst occurrences (FO) of the genera Similiscutum(jamesoni AZ) and Lotharingius (stokesi AZ). During thelate Pliensbachian, the assemblages change remarkably dueto 1) the FO of the genus Biscutum (davoei AZ), 2) an increase in abundance of Schizosphaerella, Calcivascularisand Lotharingius, 3) a decrease in abundance of Crepidolithus and Parhabdolithus and, 4) the first common occurrence (FCO) of C. jansae and L. hauffii. Related to thesecomposition changes, we have recognized and calibrated
against the ammonite zones and subzones, two main events(the FO of S. cruciulus and the FO of L. hauffii) and six
secondary events (1. FO of B. novum; 2. FO of B. grandis;
3. FO of B. finchii; 4. FO of L. barozii; 5. FCO of C. jansae;
6. FCO of L. hauffii). In the Camino and San Andrés sections, we have also identified the FOs of B. dubium, Bussonius prinsii and L. sigillatus.
The first zone recognized is the NJ3 Crepidolithus crassus (Bown, 1987) Bown & Cooper (1998), including thetime interval from the FO of C. crassus to the FO of S. cruciulus. This zone is dominated by the genera Orthogonoides and Schizosphaerella spp. and shows anincrease in the abundance of Crepidolithus and Parhabdolithus.
The base of the NJ4 Similiscutum cruciulus Zone Bown
(1987), emend. Bown & Cooper (1998), is defined by the
FO of S. cruciulus within the jamesoni AZ, as it is observedin NW Europe, Portugal and Italy. The assemblages of thiszone show an abundance increase of the genera Calcivascularis and Biscutum, and a decrease of Crucirhabdus,
Crepidolithus and Parhabdolithus. In this zone, the last occurrences of C. pliensbachensis and P. robustus, and the
Figure 1: Sketch showing ammonite zones and calcareous nannofossil
zones, with zonal and secondary events, in the Basque-Cantabrian Basin(present study), NW Europe (Bown & Cooper, 1998), and the Lusitanian
Basin (Veiga de Oliveira et al., 2007)

Abstracts

FO of the genus Biscutum have been identified. In NW Europe and Portugal, the NJ4 Zone is divided in two subzones
based on the LO of P. robustus, that in the BCB shows low
abundances and a discontinuous record. In our sections, theNJ4 Zone can be subdived using the FO of B. novum.
The base of the NJ5 Lotharingius hauffii Zone Bown
(1987) is defined by the FO of L. hauffii (stokesi AZ). In
NW Europe, this event lies in the margaritatus AZ, which
includes the stokesi and margaritatus AZs of the BCB. In
Portugal, it has been recognized in the uppermost levels of
the spinatum AZ. The lower part of the NJ5 Zone is characterized by the abundance decrease of Crepidolithus andSimiliscutum, and the increase of Calcivascularis, Biscutum and Lotharingius. This last genus shows an increase inabundance and diversity along the late Pliensbachian, related to the FOs of L. barozii and L. umbriensis (margaritatus AZ), and the FCO of L. hauffii and FO L. sigillatus(spinatum AZ). In NW Europe, the NJ5 Zone is divided in
two subzones, based on the FO of C. impontus also used in
Portugal. Because of the difficulty to distinguish C. impontus from C. cavus, and the low abundance and discontinuous record of the first species in the BCB, it seems to
be useful to divide this zone using the FO of L. sigillatus,
as proposed by Mattioli & Erba (1999) for the NJT5b subzone.
In summary, the scheme of Bown & Cooper (1998) for
NW Europe is reproducible also in the BCB, where it ispossible to calibrate the bases of NJ4 and NJ5 zones withrespect to the ammonite subzones. Though in the BCB, theNJ4a/NJ4b and NJ5a/NJ5b boundaries are not easily recognizable. The FOs of B. novum and L. sigillatus are helpful to subdivide the NJ4 and NJ5 zones, respectively.
This work was supported by the research project CGL
2005-01765/BTE and an UCM research fellowship.
References
Bown, P.R. 1987. Taxonomy, evolution, and biostratigraphy of
Late Triassic-Early Jurassic calcareous nannofossils. Special
Papers in Palaeontology, 38: 1-118.
Bown, P.R. & Cooper, M.K.E. 1998. Jurassic. In: P.R. Bown
(Ed.). Calcareous Nannofossil Biostratigraphy. Kluwer Academic, London: 34-86.
Mattioli, E. & Erba, E. 1999. Synthesis of calcareous nannofossil events in Tethyan Lower and Middle Jurassic successions.
Rivista Italiana di Paleontologia e Stratigrafia, 105(3): 343376.
Perilli, N. & Comas-Rengifo, M.J. 2002. Calibration of Pliensbachian calcareous nannofossil events in two ammonite-controlled sections from Northern Spain. Rivista Italiana diPaleontologia e Stratigrafia, 108(1): 133-152.
Veiga de Oliveira, L.C., Duarte, L., Lemos, V.B., Comas-Rengifo,
M.J. & Perilli, N. 2007. Bioestratigrafia de nanofósseis
calcários e correlação com as zonas de amonites do
Pliensbaquiano-Toarciano basal (Jurássico Inferior) de
Peniche (Bacia Lusitânica, Portugal). In: de Souza Carvalho
et al. (Eds). Paleontologia, Cenários de Vida. Interciência,
Rio de Janeiro, 2: 411-420.

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60

Abstracts

Correlation between Paratethys-Mediterranean (NN-MNN)
calcareous nannoplankton zonations
Ines Galoviç
In many cases, the nannofossil zonal-markers for the Sarmatian, i.e. Serravalian to Tortonian, are absent or rare in
sediments of the Paratethys and Mediterranean regions. It
is often difficult to correlate the Paratethys calcareous nannofossils zonation to the Mediterranean one because assemblage, abundance and bio-horizons of a certain numberof species/genera are somewhat different.
The Badenian/Sarmatian boundary in Central
Paratethys is identified on the basis of abundance and firstoccurrence of certain species/genera. Namely, close to the
top of NN6 zone or close to the base of NN7 zone, Cyclicargolithus floridanus decreases in abundance or disappears, and is replaced in the assemblage by abundant, large
R. pseudoumbilicus (≥ 7 μm) (Perch-Nielsen, 1985). This
event is reported in some other basins at different stratigraphic levels (Raffi et al., 1995). The last occurrence (LO)of Cyclicargolithus floridanus is noticed somewhat earlier
in the Mediterranean than in the Paratethys (Mărunţeanu,
1999; Hilgen et al., 2003). Its LO also differs between theCentral and Eastern Paratethys. The first occurrence (FO)of Calcidiscus pataecus, which is significant for the Lower
Sarmatian of the Croatian Basin, differs within theParatethys as well. Its FO in the Transylvanian Basin ischaracteristic for the end of the Badenian NN6d zone
(Chira & Mărunţeanu, 2000), the same as in the investigated area (Slavonian Mts). In the Vienna Basin, the FO of
C. pataecus is noticed at the beginning of the Sarmatian (S.
Ćorić, pers. comm., 2008).
A first, rare appearance of Discoaster cf. D. kugleri in
Mediterranean sapropel sediments (8.05 m in thickness) is
detected at 11.88-11.91 Ma (Ancona, Italy). Its LO is at
11.6 Ma, (Hilgen et al., 2003). Based on astronomical data,
the Serravalian/Tortonian boundary has been calibrated at
11.6 Ma. Nevertheless, the last appearance/disappearanceof Discoaster aulakos, D. deflandrei and H. walbersdorfensis in the Mediterranean region is within the NN7 zone
(Iaccarino et al., 2001). However, later investigations locate the LO of H. walbersdorfensis species at 10.74-10.76
Ma (Hilgen et al., 2003), which is in contradiction with earlier mentioned duration of NN7 zone for the Mediterranean
region. Radiometric analyses of the Central and Eastern
Paratethys are given by Vass (1999), who made numericalcalibration with Berggren’s records (Berggren et al., 1995).
Considering the rare occurrence of Discoaster kugleri insediments they placed the NN 7 zone between 11.85 – 11.3
(10.9) Ma. In the North Croatia Basin, the LO of H. walbersdorfensis species is detected at the end of the Lower
Sarmatian; this record supports a different distribution of
the species in the Paratethys.
Catinaster coalitus, whose FO defines the base of theNN8 zone, is rare or absent in many Mediterranean sections. The last occurrence of Coccolithus miopelagicus has

been detected a little earlier than this event (NN7/NN8zone), before the first occurrence of Discoaster hamatus in
the Mediterranean. Thus the LO of Coccolithus miopelagicus could be considered as an alternative marker for the
NN7/NN8 boundary (Marino & Flores, 2002). This event
belongs to ‘Chron C5r’ (Hilgen et al., 2000) that happened
at 11.2 Ma based on astronomical data for the Mediterranean region (Aguilar et al., 2004). In the North Croatian
Basin, the LO of Coccolithus miopelagicus is also observedat the NN7/NN8 boundary.
The FO of Catinaster coalitus in the Mediterranean isobserved at 10.73-10.74 Ma (Hilgen et al., 2003). Radiometric analyses from the Paratethys (Poland and Eastern
Slovakian Basin) placed the period between 11.3-10.9 Ma(Vass, 1999; Kováč et al., 2001).
The first appearance of D. hamatus in the Romanianpart of the Paratethys is found in the NN9 zone, which corresponds to the Mediterranean Serravalian/Tortonianboundary (Mărunţeanu, 1999). This bioevent is recorded
at 10.15 Ma in the Mediterranean. The Serravalian/Tortonian boundary is put at 11.6 Ma for the Mediterranean andlow-latitude ocean (Hilgen et al., 2003). Lack of reliablemagnetostratigraphy data for the boundary interval in otherregions may cause misfits in correlations. The reason forthe different FO might also be the reduction of connection
between the Mediterranean and Paratethys at the end of theSarmatian, and the re-opening of connections during the
Pannonian. Further studies on magnetostratigraphy and astronomical cycles should give us a better understanding ofcorrelations.
The paleomagnetic measurements in the Našice section(Slavonian Mts.) put the Sarmatian/Pannonian boundary at
Chron C5r.1r, which corresponds to 11.1 Ma (Agusti et al.,
2001; Vasilev, 2006). It is obvious that the Sarmatian/Pannonian boundary, previously placed at 11.6 Ma in theParatethys, needs to be revised.
References
Aguilar, J.-P., Berggren, W.A., Aubry, M.-P:, Kent, D.V., Clauzon,G., Benammi, M. & Michaux J. 2004. Mid-Neogene
Mediterranean marine - continental correlations: analternative interpretation. Palaeogeography, Palaeoclimatology, Palaeoecology, 204: 165-186.
Agustí, J., Cabrera, L., Garcés, M., Krijgsman, W., Oms, O. &Parés, J.M.A. 2001. Calibrated mammal scale for the Neogene of Western Europe, State of the art. Earth-Science Reviews, 52: 247–260.
Berggren, W.A., Kent, D.V., Swisher, C.C. & Aubry, M.-P. 1995.
A revised Cenozoic geochronology and chronostratigraphy,
In: W.A. Berggren et al. (Eds). Geochronology, Time Scales
and Global Stratigraphic correlations: A Unified Temporal
Framework for an Historical Geology. Soc. Econ. Paleont.

Abstracts
Miner., Spec. Pub., 54: 126pp.
Chira, C.M. & Mărunţeanu, M. 2000. Calcareous nannofossils
and dinoflagellates from the Middle Miocene of the Transylvanian Basin, Romania. Journal of Nannoplankton Research,
22(2): 89-90.
Hilgen, F.J., Aziz, H.A., Krijgsman, W., Raffi, I. & Turco E. 2003.
Integrated stratigraphy and astronomical tuning of the Serravalian and lower Tortonian at Monte dei Corvi (Middle –Upper Miocene, northern Italy). Palaeogeography, Palaeoclimatology, Palaeoecology, 199: 229-264.
Hilgen, F.J., Krijgsman, W., Raffi, I., Turco, E. & Zachariasse,
W.J. 2000. Integrated stratigraphy and astronomical calibration of the Serravallian/Tortonian boundary section at Monte
Gibliscemi, Sicily. Marine Micropalaeontology, 38: 181-211.
Iaccarino, S.M., Foresi, L.M., Mazzei, R. & Salvatorini, G. 2001.
Calcareous plankton biostratigraphy of the Miocene
sediments of the Tremiti Islands (S Italy). Revista Española deMicropaleontologia, 33(2:) 237-248.
Kováč, M., Nagymarosy, A., Holcova, K., Hudáčková, N., Zlinska, A. 2001. Paleogeography, paleoecology and eustacy:
Miocene 3rd order cycles of relative sea-level changes in theWestern Carpathian - North Pannonian basins. Acta Geol.
Hungarica, 44(1): 1-45.
Marino, M. & Flores, J.-A. 2002. Miocene to Pliocene calcareous
nannofossil biostratigraphy at ODP Leg 177 Sites 1088 and1090. Marine Micropaleontology, 45: 291-307.
Mărunţeanu, M. 1999. Litho- and Biostratigraphy (calcareous
nannoplankton) of the Miocene deposits from the outher Moldavides. Geol. Carpathica, 50(4): 313-324.
Perch-Nielsen, K. 1985. Cenozoic calcareous nannofossils. In:
H.M. Bolli, K. Perch-Nielsen & J.B. Saunders (Eds). Plankton stratigraphy. Cambridge University Press, Cambridge:
811-846.
Raffi, I., Rio, D., D’atri, A., Fornaciari, E. & Rocchetti, S. 1995.
Quantitative distribution patterns and biomagnetostratigraphy
and astrobiochronology of Middle to Late Miocene calcareous nannofossils from equatorial Indian and Pacific Oceans(Legs 115, 130 and 138). Proceedings ODP, Scientific Results, 138: 479-502.
Vasiliev, I. 2006. A new chronology for the Dacian Basin (Romania). Consequences for the kinematic and paleoenvironmental evolution of the Paratethys region. Geologica
Ultraiectina, 267: 193pp.
Vass, D. 1999. Numeric age of the Sarmatian boundaries (Suess
1866). Slovak Geol. Mag., 5(3): 227-232.

61

62

Abstracts

Biostratigraphic study of Middle and Upper Miocene
nannofossils from the eastern Paratethys (Tamanskii
Peninsula and northern Ciscaucasia)
Larisa Golovina
The main problem with stratigraphy of the Neogene eastern Paratethyan sediments is the correlation of its regional
stages with the central Paratethys and Mediterranean units,
as well as with standard nannoplankton NN zones. Problems in correlation of calcareous nannofossils in the
Konkian, Maeotian and Pontian regional stages have notyet been successfully resolved (Krasheninnikov et al.,2003).
Calcareous nannofossils were investigated in the deepsea sections of the Middle and Upper Miocene sediments.

The sections of the Zelenskii Mountain anticline in the
Tamanskii Peninsula and on the Pshekha River are among
the most complete Miocene sections of the eastern
Paratethys in Russia. The section on the Pshekha River belongs to the Afips-Pshekha structural facies subzone of theWest Caucasian zone, which occurs in the Psekups–
Pshekha–Kurdzhips interfluve. The high-resolution, bedby-bed studies of the Konkian have established thepresence of Braarudosphaera bigelowii, Calcidiscus macintyrei, Coccolithus pelagicus, Cyclicargolithus floridanus,
Cricolithus jonesii, Helicosphaera carteri,
Helicosphaerasp.,
Reticulofenestra
pseudoumbilica, Rhabdosphaera pannonica,
Rhabdosphaera sicca,
Rhabdosphaera sp. andSphenolithus
moriformis. The impoverished, compared to theoceanic assemblages,
nannoplankton complex
lacks
zonal
species. The most diverse assemblage occurs in a thin interval
and is correlated with
the Sartagan Beds; subsequently it became
rapidly impoverishedand was replaced bythemonospecific
Reticulofenestra
pseudoumbilica assemblage. The abundanceofReticulofenestra
coccoliths is so greatthat they became rockforming and make up a
1-m-thick marker marlbed traceable from theTamanskii Peninsula in
the west to the Pshekha
River (Northern Ciscaucasia) in the east
(Golovina et al., 2004).
This interval is correlatedwith
theVeselyanka Beds. The

Abstracts

flourishing of Reticulofenestra pseudoumbilica was most
likely associated with a frontal contact zone of fluvial andmarine waters or with the upwelling zone. Therefore, in thestudied region, the Konkian stage terminated with peculiar
bionomic conditions.
Calcareous nannofossils from the Maeotian and Pontian deposits in the Tamanskii Peninsula (Taman’ and Iron
Horn sections) are represented by poor assemblages bearing only one or two genera and likely indicating shallowwater and/or nearshore conditions; they are mostly of nobiostratigraphic value. The Upper Maeotian deposits contain a great number of specific calcareous elements that in
our opinion belong to the ascidian spicules. The abundantascidian spicules are an excellent indicator of sublittoraland littoral conditions of sedimentation. Transition from
the Maeotian to Pontian is characterized by a powerful development of monospecific Braarudosphaera bigelowii assemblages along with the diatom monospecific
Actinocyclus ehrenbergii assemblages. These deposits
mark a zone of the ancient hydrological front. Cyclicity ofhydrological conditions is excellently illustrated by alternation of nannoplankton and diatom monospecific assemblages.
This work was supported by the Russian Foundationfor Basic Research, project nos 06-05-64049-а and 07-0500795-а.
References
Golovina, L.A., Goncharova, I.A. & Rostovtseva, Y.V. 2004. New
Data on the Middle Miocene Biostratigraphy (Nannofossils,
Mollusks) and Lithology of the Tamanskii Peninsula andWestern Ciscaucasia. Stratigraphy and Geological Correlation, 12(6). MAIK “Nauka/Interperiodica” Publishing: 637646.
Krasheninnikov, V.A., Basov, I.A. & Golovina, L.A. 2003.
Tarkhanian and Konkian Regional Stages of the Eastern
Paratethys (Stratigraphy, Micropaleontology, Bionomy, Paleogeographic Connections). Nauchnyi Mir, Moscow.

63

64

Abstracts

Calcareous nannofossil biostratigraphy of the Gurpi
Formation in the Kangan Anticline
Fatemeh Hadavi
The Zagros bBasin is situated in southwestern Iran, the region known as the 1954 Agreement Area. The northwestern limit of this region coincides with the well-known
tectonic zone called the ‘Main Zagros Thrust’. The southwestern limit coincides with the southwestern boundary of
Iran. Several thousand meters of carbonate, siliciclastics
and evaporites were deposited in the Zagros Basin. These
sediments are folded into simple anticlines and synclines.
The basin is one of the biggest oilfields in the world.
The Gurpi Formation is one of the most complete Early
Santonian – Early Danian sequences, and it is widespreadover most of the Agreement Area, although it displays lateral changes in lithology. This study focuses on the Gurpi
Formation in Kangan Anticline. In this area, the Gurpi Formation consists of 100 m of bluish-gray marls with intercalation of marly limestone. The Gurpi Formation is incontact (disconformity) on the Ilam Formation that is represented by thin-bedded limestone with intercalation of
nodular shale, and it is overlain in disconformity by the
Pabdeh Formation. Between the Gurpi and Pabdeh Formations, 30 cm of glauconite-rich sediments area present.
Calcareous nannofossils of this formation were studied
in different localities by Hadavi et al. (2007). This study
focuses on the boundary between the Gurpi and Pabdeh
Formation. According to the presence of Micula murus andBiantholithus sparsus in the glauconites, the boundary isplaced in the uppermost part of the Gurpi Formation. On
the other hand the presence of Discoaster multiradiatus,
Discoaster bramlettei in the lower Pabdeh Formation is
discontinuous in this area.
References
Hadavi, F., Khosrowtehrani, K. & Senmari, S. 2007. Biostratigraphy of calcareous nannofossil biostratigraphy of
the Gurpi Formation in north Gachsaran. Scientific
Quarterly Journal. Geo. Surv., Iran.

Abstracts

65

Pseudocryptic speciation of living Braarudosphaera
bigelowii
Kyoko Hagino, Yoshihito Takano, Takeo Horiguchi
Notable size variations have been reported from living andfossil populations of Braarudosphaera bigelowii (Gran &Braarud, 1935) Deflandre (1947), however, size factor has
not been integrated in the taxonomy of B. bigelowii due tolack of genetic evidence (Hagino, 1997; Svábenická, 1999;
Konno et al., 2007). Takano et al. (2006) subdivided theliving B. bigelowii population into three morphotypes;
Small forms, Intermediate forms –A and –B, based on sizeof the pentaliths. They obtained SSU rDNA sequences of
two natural cells of B. bigelowii based on the single-cell
PCR technique, and found 16-bp differences, including indels between the cells belonging to Intermediate form-A
and Intermediate form-B. However, they did not emend
their taxonomic position, since the size range of these twoforms overlapped.
To examine the taxonomic position of morphotypes ofliving B. bigelowii, we studied sufficient number of living
cells of B. bigelowii from various parts of Japan, genetically. In this study, partial SSU rDNA sequences (>1600bp) of 14 cells of B. bigelowii, which were different in size,
were obtained using the single-cell PCR technique. In
addition to the previously reported three morphotypes by
Takano et al. (2006), a new morphotype, Intermediate form
–C (>7.0μm in side length of pentalith), was recognized.
Together with the sequences reported by Takano et al.
(2006), the number of specimens of Intermediate forms -A,-B and -C sequenced increased to six, seven and three, respectively. Signature sequences that represent Intermediate
forms –A, –B and –C were found; ten substitutions separate
Intermediate forms –A and –B from each other, and an additional one substitution separates Intermediate form–Cfrom Intermediate form–B. SSU rDNA sequences of sevenspecimens belonging to the Intermediate form-B were consistent. However, one additional substitution was foundfrom one of the Intermediate form–A cells and also fromone of the Intermediate form–C cells, regardless of sampling area.
SSU rDNA sequence types were correlated with morphotypes classified based on size, not on sampling area.
Therefore, it is evident that the Intermediate forms A-C are
genetically distinct species. Since the Intermediate form-B
corresponds in size to the original description by Gran &Braarud (1935), Intermediate forms –A and –C should beraised to species rank.
References
Deflandre, G. 1947. Braarudosphaera nov. gen., type d’une
famille nouvelle de Coccolithophoridés actuels à elementscomposites. C. R. Hébd. Séances Acad. Sci., Paris, 225: 439–
441.
Gran, H.H. & Braarud, T. 1935. A quantitative study of the phytoplankton in the Bay of Fundy and the Gulf of Maine (in-cluding observations on hydrography, chemistry and turbidity). J. Biol. Board Can., 1(5): 279–467.
Hagino, K. 1997. Distribution of living coccolithophores in thewestern Pacific Ocean off the coast of Northeast Japan. Fossils, 63: 1-19.
Konno, S., Harada, N., Narita, H. & Jordan, R.W. 2007. Living
Braarudosphaera bigelowii (Gran & Braarud) Deflandre in
the Bering Sea. J. Nannoplankton Res., 29(2): 78-87.
Svábenická, L. 1999. Braarudosphaera-rich sediments in the Turonian of the Bohemian Cretaceous Basin, Czech Republic.
Cretaceous Res., 20: 773-782.
Takano, Y., Hagino, K., Tanaka, Y., Horiguchi, T. & Okada, H.
2006. Phylogenetic affinities of an enigmatic nannoplankton,
Braarudosphaera bigelowii based on the SSU rDNA sequences. Mar. Micropaleontol., 60: 145-156.

66

Abstracts

Calcareous nannofossil study of a possible West Carpathianregional stratotype profile of the Jurassic/Cretaceous
boundary (the Brodno section, near Zilina)
Eva Halásová
This contribution presents some results on calcareous nannofossils in the Brodno section, a possible candidate for aWestern Carpathian regional J/K boundary stratotype. The
continuous Jurassic-Cretaceous pelagic limestone sequenceof the Brodno section offers the possibility to document theJ/K passage in a wide area of the Western Carpathians. The
Brodno section is situated in an ancient quarry on the eastern side of the narrow straits of the Kysuca River Valley,
north of the town of Zilina (NW Slovakia). It yields arecord of hemipelagic marine sedimentation in a marginalzone (the Pieniny Klippen Belt) of the Outer Western
Carpathians. The Late Jurassic sedimentation rate in the
Pieniny Klippen Belt was low. The condensed red nodular
limestones of the ‘Ammonitico Rosso Facies’ (the Czorsztyn Formation), which represent the Kimmeridgian andTithonian part of the Kysuca Succession, received only alimited terrigenous clastic input. During the Berriasian,subsiding West Carpathian basins were affected by a great
acceleration in the ‘planktic rain’ of organic matter and calcareous microskeletons. This change produced pelagic sediments of the ‘maiolica’ type (the Pieniny Limestone
Formation). This sedimentary pattern persisted until the
Early Aptian in the Pieniny Klippen Belt.
Calcareous nannofossils were analyzed in 40 smear
slides prepared from all the lithologies under a light microscope at 1250x magnification. The abundance was determined by counting all specimens in at least 200 fields ofview in each sample. The preservation of the fossil material has been characterized as moderately to heavily etchedby dissolution.
Calcareous nannofossils form relatively low-diversity
associations. Eighteen nannofossil species were recognised. The coccolithophorids are represented by Watznaueriaceae: Watznaueria barnesiae, W. britannica, W.
manivitiae, W. ovata, Cyclagelosphaera margerelii and C.
deflandrei. Zeugrhabdotus embergeri is also frequently
recorded. Dissolution-resistant coccolith taxa, such as Helenea chiastia, Cruciellipsis cuvillieri, and other more delicate taxa, such as Z. erectus, Diazomatolithus lehmanii andDiscorhabdus ignotus occur more sporadically. Nannoliths
Conusphaera mexicana mexicana, C. mexicana minor,
Polycostella beckmannii, Assipetra spp., Hexalithus
noeliae, Lithraphidites carniolensis, Nannoconus infans,
N. wintereri, N. steinmanni minor, N. globulus minor andN. kamptneri minor are also present. Abundance fluctuations of dissolution-resistant nannoliths (Conusphaera,
Polycostella, Nannoconus) and coccoliths (C. margerelii,
W. barnesiae, W. manivitiae) have been detected by quantitative study. The nannofossil zonation of Bralower et al.
(1989), as modified by Tavera et al. (1994), was used. Two

nannozones, the C. mexicana mexicana and H. chiastia
zones, were distinguished in the Western Carpathians. Calcareous nannofossils from the lower half of the studied sequence (L52 to L96) are correlated with the Early to middle
Tithonian C. mexicana mexicana Zone (NJ20). This zone
comprises the P. beckmanii Subzone; the latter one consistsof the H. noeliae, or NJKA, NJKB and NJKC subzones.
For this section, calpionellid stratigraphy is also available, along with older paleomagnetic data. Calcareous nannofossils formed poorly diversified associations at the J/Kboundary. The abundance of Watznaueria, Cyclagelosphaera, Conusphaera and Polycostella species inthe section studied is relatively high. Other nannofossils
are rather rare. Conusphaera predominates in the Tithonian(showing a Middle Tithonian peak). Polycostella increased
in abundance during the Boneti Subzone of the Chitinoidella Zone. The Middle/Late Tithonian boundary was
detected by means of the FO of H. chiastia accompanied by
the first small nannoconids. Small nannoconids appeared in
the Late Tithonian and increased in size and abundance
during the Berriasian. Polycostella diminished in abundance towards the onset of the Crassicollaria Zone. The
Late Tithonian interval was delimited by the FOs of L.
carniolensis, N. infans, N. wintereri and C. cuvillieri within
the H. chiastia Zone, which is correlated with the standard
Crassicollaria Zone. From the point of view of nannofossil stratigraphy, the Tithonian/Berriasian boundary interval
should be placed between the FO of N. wintereri (Sample
C17, Upper Tithonian) and the FO of N. steinmanni minor(Sample C28, lowermost Berriasian). In this interval, theonset of the Alpina Subzone of the standard calpionellid
zonation is also recorded (the C23A-C25A beds), whichcorresponds to the calpionellid J/K boundary zone.
Sequence stratigraphy and stable isotope (δ18O, δ13C)
data also provided good results, enabling the studied section to be compared to important key sections in the
Mediterranean Tethys area.
This is a contribution to the 506 IGCP UNESCO Project, supported by VEGA grant projects 6026, 2035 and
3178, APVV-0465-06, APVT 51-011305 and Project
APVV - 0280-07.
References
Bralower, T.J., Monechi, S. & Thierstein, H.R. 1989. Calcareous
nannofossil zonation of the Jurassic-Cretaceous boundary interval and correlation with the geomagnetic polarity
timescale. Marine Micropaleontology, 14: 153-235.
Tavera, J.M., Aguado, R., Company, M. & Olóriz, F. 1994. Integrated biostratigraphy of the Durangites and Jacobi Zones(J/K boundary) at the Puerto Escaño section in southern Spain(Province of Cordoba). Geobios, 17: 469-476.

Abstracts

67

Environmental control on size and genotype of Emiliania
huxleyi
Jorijntje Henderiks, Amos Winter, Malte Elbrächter, Anja van der Plas, Rainer
FeistelCoccolithophores play an important role in the
global carbon cycle as primary producers andmarine calcifiers. Because of ocean acidification due to increased atmospheric CO2 weneed to constrain how natural coccolithophore
populations can acclimatize or adapt to projected changes, and how their natural feedback
mechanisms may operate in future. In recent
years, numerous experimental studies havehighlighted environmental controls on coccolith calcification and malformation, mostly
using monoclonal cultures of Emiliania huxleyi (e.g. Paasche et al., 1996; Paasche, 1998;
Riebesell et al., 2000; Sorrosa et al., 2005;
Iglesias-Rodriguez et al., 2008). However, extrapolating laboratory-based results to thescales and dynamics of the ‘real’ ocean remains speculative. The upwelling region offFigure 1: Examples of living E. huxleyi sampled offshore Namibia. a) Type A heavily calshore Namibia, characterized by small-scale cified, large coccosphere; b, c) Type A coccospheres with malformed coccoliths; d) Typebut large gradients in temperature, nutrient B/C with delicate distal shield elements and open central areas. Scale-bar = 2μm
availability and CO2 concentrations, serves asa scenario where E. huxleyi populations thrive under elea natural laboratory where we can test hypotheses convated levels of dissolved inorganic carbon (DIC), althoughcerning the environmental controls on coccolith calcificanitrate deficiency and/or lower calcite saturation/ocean pHtion/malformation and ecological responses in natural
may contribute to extensive coccolith malformation in thispopulations.
upwelling region.
Here we present coccolithophore and in situ environmental data from water-column samples collected during
References
cruise 48/5 of the RV Meteor (October 2000) from transect
Iglesias-Rodriguez, D., Halloran, P.R., Rickaby, R.E.M., Hall, I.,lines perpendicular to the Namibian coast. Samples coverColmenero-Hidalgo, E. & others 2008. Phytoplankton calcia wide spectrum, from recently upwelled waters to oceanic
fication in a high-CO2 world. Science, 320: 336-340.
surface waters. Closest to shore in recently upwelled wa- Paasche, E. 1998. Roles of nitrogen and phosphorus in coccolithters, large blooms of diatoms dominate the phytoplankton
formation in Emiliania huxleyi (Prymnesiophyceae). Eur. J.
biomass. E. huxleyi is the most dominant species in older
Phycol., 33: 33-42.
upwelling waters above the shelf edge and slope. Coccol- Paasche, E., Brubak, S., Skattebøl, S., Young, J.R. & Green, J.C.
1996. Growth and calcification in the coccolithophorid Emiliths in these waters were often malformed. Two different
iania huxleyi (Haptophyceae) at low salinities. Phycologia,
morphotypes (likely genotypes) of E. huxleyi occurred in
35(5): 394-403.
environmentally distinct zones (Fig. 1). E. huxleyi with delRiebesell, U., Zondervan, I., Rost, B., Tortell, P.D., Zeebe, R.E. &icate distal shield elements and open central areas (TypeMorel, F.M.M. 2000. Reduced calcification of marine plankB/C cf. Young et al., 2003) dominated in highly nitrogenton in response to increased atmospheric CO2. Nature, 407:
depleted surface waters above the continental slope. At
364-367.
these stations, cell abundances reached 300x103 cells/liter. Sorrosa, J.M., Satoh, M., Shiraiwa, Y. 2005. Low temperature
More heavily calcified E. huxleyi (Type A cf. Young &stimulates cell enlargement and intracellular calcification of
coccolithophorids. Marine Biotechnology, 7(2): 128-133.
Westbroek, 1991) were dominant at stations above the shelfedge and slope, with cell abundances ranging from 2000 to Young, J.R., Geisen, M., Cros, L., Kleijne, A., Sprengel, C.,
Probert, I. & Østergaard, J. 2003. A guide to extant coccol>106 cells/liter. Most populations of E. huxleyi Type A wereithophore taxonomy. J. Nannoplankton Res., Special Issue, 1:
malformed, with irregularly arranged distal shield elements
8.
that appear detached from a central coccolith rim. A bloom
Young, J.R. & Westbroek, P. 1991. Genotypic variation in the cocof anomalously large Type A coccospheres with well-decolithophorid species Emiliania huxleyi. Marine Micropaleveloped and heavily calcified coccoliths was observed in
ontology, 18: 5-23.
relatively cool water where nutrient concentrations werecloser to the Redfield N:P ratio. Our observations suggest

68

Abstracts

Response of coccolith size to paleoceanographic changes
during the Pliocene at Site 999A, Southern Caribbean Sea
Sandra Herrmann, Gretta Bartoli, Andrew F. Weller, Hans R. Thierstein
Our studies of global Holocene surface sediments havedemonstrated that temperature is the dominant factor controlling coccolith size variability in Recent assemblages.
However, the role of other parameters, such as salinity, pH
and pCO2 has not been completely decoded. We have now
compared the coccolith size variability with environmental
parameters in the Holocene to the response to paleoceanographic changes during the Pliocene Epoch in order to disentangle the multiple environmental dependencies and topossibly identify evolutionary adaptations.
Site 999A in the Caribbean Basin was chosen becauseof its excellent carbonate preservation and the broad variety of data available on ocean circulation patterns, environmental parameters and nannofossil assemblages. We
investigated a period from 5 to 2 Ma with a ~30 kyr resolution. The age model used was taken from Steph et al.
(2006) and re-tuned to the benthic δ18O stack LR04 from
Lisiecki & Raymo (2005). Samples were prepared on SEM
stubs according to a specific spraying method (Henderiks& Törner, 2006), image frames of coccoliths were captured
in a Philips XL30 SEM with an automated scanning module. The frame series were then automatically segmented
and the maximum sizes of coccoliths measured.
Our Pliocene study indicates a general decrease of coccolith size between 5 and 2 Ma. Additionally, strong variations in coccolith sizes are recorded during 4.3-3.8 Ma
and 2.9-2.5 Ma. The older of these intervals of coccolith
size change might be related to the temperature change
recorded in benthic δ18O records (Lisiecki & Raymo,2005). The interval 2.9 to 2.5 Ma equals the period of theclosure of the Panamanian Seaway, which was causing areorganization of paleoceanographical settings in the
Caribbean Sea and thus might be reflected in size changes
in the plankton assemblage.
References
Henderiks, J. & Törner, A. 2006. Reproducibility of coccolithmorphometry: Evaluation of spraying and smear slide preparation techniques. Marine Micropaleontology, 58: 207-218.
Lisiecki, L.E. & Raymo, M.E. 2005. A Pliocene-Pleistocene stackof 57 globally distributed benthic δ18O records. Paleoceanography, 20: PA1003, doi:10.1029/2004PA001071.
Steph, S., Tiedemann, R., Prange, M., Groeneveld, J., Nürnberg,D., Reuning, L., Schulz, M. & Haug, G.H. 2006. Changes in
Caribbean surface hydrography during the Pliocene shoalingof the Central American Seaway. Paleoceanography, 21:
PA4221, doi:10.1029/2004PA001092.

Abstracts

69

Millennial-scale paleoenvironmental changes in the central
Mediterranean during the Last Interglacial: comparison
with European and North Atlantic records
Alessandro Incarbona, Sergio Bonomo, Enrico Di Stefano, Rodolfo Sprovieri,
Nicola Pelosi, Mario Sprovieri
The occurrence and the meaning of high-frequency climatic fluctuations from the upper part of MIS 6 to thelower part of MIS 4 in Hole 963A (37˚01.938’N,
13˚10.896’E, central Mediterranean Sea) have already been
discussed, on the basis of high-resolution planktonic
foraminifera and calcareous nannofossil data (mean sampling resolutions, respectively, of about 80 and 160 yr), andof benthic and planktonic oxygen isotope records(Sprovieri et al., 2006). Here we show the distribution patterns of other 8 planktonic foraminifera and 6 calcareous
nannofossils with the aim to investigate the marine environment of the Sicily Channel during MIS 5, mainly interms of temperature and stability of the water column.
Both calcareous plankton groups show a co-ordinatedresponse to environmental changes, as demonstrated bysignificant correlation indexes among the main taxa. For
instance, Gephyrocapsa muellerae is anti-correlated to
Globigerinoides ruber (-0.77, n = 401) and to Florisphaera
profunda (-0.7, n = 401). MIS 5 is generally characterized
by warm, oligotrophic and stratified waters, where coccolithophore communities developed a vertical zonation. In
today’s oceans, a similar vertical zonation is typical of the
low-latitude gyres (Winter et al., 1994). The temperate-subtropical assemblages of planktonic foraminifera and calcareous nannofossils repeatedly changed into
temperate-subpolar assemblages during the suborbital cooling episodes C25-C18.
A comparison with European pollen sequences andNorth Atlantic cores over the interval between ~128 and
110 kyr BP has been performed. Records from this broad
geographical area show a series of environmental changes
that occurred at comparable times. However, the first cooling episodes were more severe at high-latitude (approximately north of 50˚N), where an earlier end of interglacialconditions can be inferred (Sánchez-Goñi et al., 2005). An
objective definition of interglacial conditions at Site 963
appears difficult, given that planktonic organisms respond
not only to water mass temperature, but to a wide range ofphysical-chemical conditions. Nevertheless, the slight increase of G. ruber and the new development of a vertical
zonation in the coccolithophore community after the C25
episode, suggest the re-establishment of weaker interglacial-like conditions, which gradually degraded until thesevere C24 event. Therefore, interglacial-like conditions
were probably maintained for 16-18 kyr. A similar duration
can be also deduced for the Alboran Sea. Such a long duration is similar to that reported from southern European
continental records, but it is in contrast with the shorter duration of the Eemian, north of the Alps.

The similarity of European/Mediterranean and North
Atlantic environmental changes during the last interglacialat about 122, 118 and 110 kyr BP, and an earlier end of interglacial conditions at higher latitudes, need to be interpreted in terms of an adequate climate-forcing model, able
to affect such a broad region as well as to generate such alatitudinal pattern. Both the southward expansion of the
Polar Vortex and disturbances in the meridional overturning circulation can explain the contemporary environmental changes across this area and the progressive
involvement of lower-latitude sites in the glaciation
process.
References
Sanchez Goñi, M.F., Loutre, M.F., Crucifix, M., Peyron, O., Santos, L., Duprat, J., Malaizé, B., Turon, J.-L. & Peypouquet,
J.-P. 2005. Increasing vegetation and climate gradient in western Europe over the Last Glacial Inception (122-110 ka): data
model comparison. Earth and Planetary Science Letters, 231:
111-130.
Sprovieri, R., Di Stefano, E., Incarbona, A. & Oppo, D.W. 2006.
Suborbital climate variability during Marine Isotopic Stage 5in the central Mediterranean Basin: evidence from calcareousplankton. Quaternary Science Reviews, 25: 2332-2342.
Winter, A., Jordan, R.W. & Roth, P.H. 1994. Biogeography of living coccolithophores in ocean waters. In: A. Winter & W.G.
Siesser (Eds). Coccolithophores. Cambridge University Press,
Cambridge: 199-218.

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Abstracts

Coccolithophorid distribution in Palauan lagoons
Atsuko Kijima, Richard W. Jordan
The Republic of Palau consists of a group of islands in theNW equatorial Pacific characterized by reefal lagoons andmarine lakes. The environmental conditions are relatively
stable throughout the year, but with a rainy (June-October)and dry (November-May) season associated with the Asianmonsoon. Since 2001, we have conducted expeditions to
Palau at least once a year, although the sampling season
has varied. Using May-July samples from three different
years, Konno & Jordan (2006) provided the first account ofa coccolithophorid community from Palau, with a low
species diversity in the lagoons, but a higher diversity inthe open sea. Abundance was also low, reaching up to 1 x
104 cells/litre, and they were always outnumbered by thediatoms. Gephyrocapsa oceanica dominated all of their 21
samples, which were collected from two marine lakes aswell as very shallow (<1 m), shallow (<5 m) and deep (upto 40 m) lagoon sites. Of the 23 spp. recorded by them, surprisingly none were holococcolithophorids. However, they
did find some rarely reported species such as Cruciplacolithus neohelis and Anacanthoica cidaris.
New observations on 65 samples collected during thedry season (November 2006 and late October 2007) werecompared with those of Konno & Jordan (2006). Gephyrocapsa oceanica dominated almost all of the samples,with its highest absolute abundances closely correlated to
low Simpson’s Index of Diversity scores, whereas species
diversity was generally highest in the more offshore waters. However, abundances (up to 5 x 103 cells/litre) in 2006
were somewhat lower than those of Konno & Jordan(2006). Of the 21 species observed in the 2006 samples, 6of them were recorded for the first time, including the holococcolithophorid Calicasphaera blokii. Of the 11 species
recorded in 2007, only two were new to Palau, Syracosphaera rotula and the holococcolithophorid Helladosphaera cornifera. So in total, 31 species have beenfound, but clearly further work is needed to fully document
the total floral composition. Expeditions to other coral reefislands within Micronesia are now being planned.
Reference
Konno, S. & Jordan, R.W. 2006. Lagoon coccolithophorids fromthe Republic of Palau, NW Equatorial Pacific. Journal of
Nannoplankton Research, 28(2): 95-110.

Abstracts

Effects of ocean acidification on the calcification of
coccolithophores – Evidence from experimental studies
Gerald Langer, Ian Probert, Björn Rost, Patrizia Ziveri
Anthropogenic CO2 emissions, and a concomitant decrease
in seawater pH, a process termed ‘ocean acidification’,
have attracted much attention in the last decade. Resultsfrom experimental studies on corals and foraminifera havelead to the hypothesis that calcification of coccolithophores
might be hampered at elevated concentrations of CO2 inseawater. This was indeed found to be true in an initialstudy using the bloom-forming species Emiliania huxleyi
and Gephyrocapsa oceanica. The relationship between
calcification rate and CO2 concentration was described bylinear regression. However, the question whether theobserved response is typical for the group of
coccolithophores, remained unanswered. Therefore, thetwo productive calcite producers Calcidiscus leptoporus
and Coccolithus pelagicus were tested. The latter species
was insensitive over the CO2 range tested, while C.
leptoporus showed an optimum curve with the highest
calcification rate at present day CO2 levels. This study
clearly demonstrated that species-specific effects play arole in coccolithophore response to altered carbonate
chemistry of seawater. More experimental studies using
species of different phylogenetic origin are clearly
warranted to obtain detailed information about the possible
effect of ocean acidification on coccolithophores.
Considering the different timescales of laboratory
experiments, and change of carbonate chemistry in theoceans, it will certainly be necessary to investigate thepotential of adaptation in these algae.

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Abstracts

Changes in photic-zone habitats through the equatorial
Atlantic Palaeocene/Eocene Thermal Maximum: contributions from species-specific nannofossil geochemistry
Jackie A. Lees, Paul R. Bown, Jeremy R. Young, Stuart Robinson, Ken
MacLeod, Darren Gröcke, Fab Minoletti
Stable isotope patterns through the Palaeocene/Eocene
Thermal Maximum (PETM) show clear distinctions between per-sample size-fractions that equate to individual
species or morphotypes of calcareous nannofossil. Geochemistry of a sequence of size-fractionated samples
through the pre- to post-PETM interval of Demerara Rise(equatorial Atlantic) reveals that the Coccolithus and Discoaster δ13C curves mimic the positive excursion, but with
the Coccolithus signal lagging behind that of Discoaster.
Toweius shows increasing δ18O prior to the PETM, whilst
Discoaster shows a pre-PETM increase and an intra-PETM
decrease. Coccolithus appears to split into two morphotypes through the PETM. A ‘medium’-sized form is more
dominant during the PETM, and shows relatively stable
δ18O values, whilst a ‘small’ form has a widely variable signal, showing first a decrease, then an increase in δ18O
through the PETM.
These data are complex and mediated by preservation,
which in these oceanic oozes is only moderate. Furthermore, data is not available for every species in each sample, due to the limitations of the fractionation technique.
Despite this, we will present our first interpretations of thepalaeoecologies of these species, based on the stable isotope data, in tandem with elemental data (hopefully), fromwhich we will hypothesise changes in the photic-zone habitats.

Abstracts

73

Evidence of increasing surface-water oligotrophy during theCampanian-Maastrichtian boundary interval: calcareous
nannofossil assemblages of DSDP Hole 390A (Blake Nose)
Christian Linnert, Jörg Mutterlose
Several stable isotope studies imply a general cooling trend
throughout the Campanian-Maastrichtian period (e.g.
Huber et al., 2002; Miller et al., 2005). Recently, this viewhas been modified with two short termed cooling events ofearly and middle Maastrichtian age, which interrupt the
progressive cooling trend (e.g. Barrera & Savin, 1999;
Thibault & Gardin, 2006). In order to better understand thisclimatic evolution, material from DSDP Site 390A has beenstudied for calcareous nannofossils. This site contains achalky, 13.8m-thick uppermost Campanian-lower Maastrichtian interval (Benson et al., 1978). Stable isotope studies on planktic foraminifera of DSDP Site 390 indicate
three minor cooling events (events A, B, C) instead of one
major event (Friedrich et al., 2004). Subsequent studies onbenthic foraminfera suggested an increasing oligotrophy
throughout this interval (Friedrich & Hemleben, 2006).
We collected 60 samples from the Campanian-Maastrichtian boundary interval. For the study of calcareous
nannofossil assemblages we used the settling technique(Geisen et al., 1999). Abundances were determined bycounting 372 to 469 specimens in each sample. Two traverses were investigated for rare species. Finally, we obtained biometrical data (coccolith length, width and centralarea) of 50 specimens of Arkhangelskiella in each sample.
The preservation of nannofossil specimens is generally
good. A total number of 118 taxa has been encountered, themean species richness is around 80 species per sample. The
absolute abundance varies between 3.74 * 109 and 11.52 *
109 (mean 6.80 * 109) specimens/g sediment. The assemblage is dominated by Prediscosphaera spp. (20.5%),
Watznaueria spp. (20.3%), Retecapsa spp. (9.8%) and Micula spp. (5.1%). Other abundant taxa are Cribrosphaerella
ehrenbergii (3.9%), Ceratolithoides spp. (3.5%) and Discorhabdus ignotus (3.3%). Around 133mbsf, several taxa
(D. ignotus, Zygodiscus exmouthiensis, Zeugrabdotus bicrescenticus) decrease, while Staurolithites flavus increases(Fig. 1). The oligotrophic taxa Watznaueria spp. and Micula spp. increase slightly around this level (Fig. 1). On the

Figure 1: Fluctuations of absolute abundance, simple diversity (= species richness), relative abundances of several nannofossil taxa (Arkhangelskiellaspp., cool-water taxa, D. ignotus, Micula spp., S. flavus, Watznaueria spp., Z. exmouthensis, Z. bicrescenticus) and the mean size of Arkhangelskielladuring the Campanian-Maastrichtian boundary interval at Hole 390A. Cool-water taxa include A. octoradiata, G. segmentatum and K. magnificus. Stable isotopes are after Friedrich et al. (2004)

74

Abstractssame level, the average length of Arkhangelskiella spp.
coccoliths increases from 6.8 to 8.7μm (Fig. 1). Cool-watertaxa (Ahmuellerella octoradiata, Gartnerago segmentatum,
Kamptnerius magnificus) are present, but their relative
abundance is always below 1%.
The oxygen isotope data of Friedrich et al. (2004) indicate three surface-water cooling events (A, B, C; Fig. 1).
The rare cool-water taxa show an increase during cooling
event B, but no significant increases during events A and B.
On the other hand, the cool-water taxa show a similar increase around 127-128mbsf. Several taxa show a turnoverat the level 133mbsf. While oligotrophic taxa, like
Watzanueria spp. and S. flavus increase, the eutrophic zeugrhabdotids decrease (Fig. 1). This suggests a turnover tomore oligotrophic surface-waters. The benthic
foraminiferal studies of Friedrich & Hemleben (2007) support this interpretation. The different sizes of Arkhangelskiella seem to correspond to ecophenotypes. In the lower
part of the succession, Arkhangelskiella is more abundant,
but the specimens are predominantly small (mean 6.8μm).
These small specimens are probably eutrophic ecophenotypes, having a r-selected life strategy. Above 133mbsf, theaverage size increases to 8.7μm, but the abundance declines. The large specimens may have been oligotrophic,
K-selected ecophenotypes. Thus the decrease in nutrientswould have caused an increase in average size. Girgis(1987) measured the length of Arkhangelskiella specimens
throughout the Maastrichtian of a Tethyan outcrop (Egypt),and observed a continuous increase in mean length from
7.4μm (Upper Campanian) to 12.5μm (Upper Maastrichtian). The abrupt increase in size of Arkhangelskiella specimens from 6.8μm to 8.7μm in DSDP Hole 390A may hint
towards a hiatus between the Upper Campanian below
133mbsf and the Lower Maastrichtian above 133mbsf.
The Campanian-Mastrichtian boundary interval isthought to be a time of massive global changes. In several
localities, a prominent cooling event occurred. In other settings, a change in nutrient influx is recorded. Our results
show a clear response of fossil coccolithophores, primary
producers, to environmental changes at the CampanianMaastrichtian transition.
References
Barrera, E. & Savin, S.M. 1999. Evolution of late CampanianMaastrichtian marine climates and oceans. In: E. Barrera &CC. Johnson (Eds). Evolution of the Cretaceous ocean climate system. Geological Society of America, Special Paper,
332: 245-282.
Benson, W.E., Sheridan, R.E., Pastourt, L., Enos, P., Freeman, T.,
Murdmaa, I.O., Worstell, P., Gradstein, F., Schmidt, R.R.,
Weaver, F.M. & Stuermer, D.H. 1978. Initial Reports of the
Deep Sea Drilling Project, 44. Washington (US Government
Printing Office).
Friedrich, O. & Hemleben, C. 2007. Early Maastrichtian benthic
foraminiferal assemblages from the western North Atlantic(Blake Nose) and their relation to paleoenvironmental
changes. Marine Micropaleontology, 62: 31-44.
Friedrich, O., Herrle, J.O., Kößler, P. & Hemleben, C. 2004. Early
Maastrichtian stable isotopes: changing deep water sourcesin the North Atlantic? Palaeogeography, Palaeoclimatology,
Palaeoecology, 211: 171-184.
Geisen, M., Bollmann, J., Herrle, J., Mutterlose, J. & Young, J.
1999. Calibration of the random settling technique for calculation of absolute abundances of calcareous nannoplankton.
Micropaleontology, 45: 437-442.
Girgis, M.H. 1987. A morphometric analysis of the Arkhangelskiella group and its stratigraphical and palaeoenvironmental
importance. In: J.A. Crux & S.E. van Heck (Eds). Nannofossils and their applications. Ellis Horwood Limited, Chichester, England: 327-339.
Huber, B.T., Norris, R.D. & MacLeod, K.G. 2002. Deep-sea paleotemperature record of extreme warmth during the Cretaceous. Geology, 30: 123-126.
Miller, K.G., Wright, J.D. & Browning, J.V. 2005. Visions of ice
sheets in a greenhouse world. Marine Geology, 217: 215-231.
Thibault, N. & Gardin, S. 2006. Maastrichtian calcareous nannofossil biostratigraphy and paleoecology in the Equatorial Atlantic (Demerara Rise, ODP Leg 207 Hole 1258A). Revue deMicropaléontologie, 49: 199-214.

Abstracts

Coccolith evidence of upper ocean water variations for the
past 1.53Myr in the Western Pacific Warm Pool
Chuanlian Liu, Shiying Zhang, Haiyan Jin
Coccolith analysis has been carried out for the past 1.53
Myr sediment from ODP Site 807, which is located in thecenter of the Western Pacific Warm Pool. The results showthat the depth of nutricline experienced significant changes,
mainly at 0.9, 0.48 and 0.28 Ma, respectively, enabling therecognition of four stages of change for the last 1.53 Myr.
From 1.53 Ma to 0.9 Ma, the depth of nutricline shoaled
gradually. At about 0.9 Ma, the nutricline abruptly
deepened and remained stable until 0.48 Ma. The nutricline
became very shallower during the time interval between
0.48 to 0.28 Ma. At 0.28 Ma, it deepened again and increased gradually up to the present. Variations in primary
productivity match with the nutricline fluctuations, and alsowith the depth of thermocline derived from planktonic
foraminifera. Comparison between the percentage of F.
profunda and primary productivity, from ODP Site 807 andODP Site 1143 in the southern South China Sea, indicates
opposite changes before 0.9 Ma, but similar changes after
0.9 Ma. This implies that variations in the upper ocean
water are different between the center and the margin of
the Western Pacific Warm Pool before 0.9 Ma, but after 0.9
Ma they have the same trends.

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Abstracts

Variability of the coccolith-derived carbonate at ODP Site
1242 in the eastern tropical Pacific during the middle andlate Pleistocene
Gatsby-Emperatriz López-Otálvaro, José-Abel Flores, Francisco Javier Sierro,
Alan C. Mix
This study is focused on the sedimentary sequence recovered during Ocean Drilling Program Leg 202 at Site 1242
on board the R/V Joides Resolution. Site 1242 is locatedin the Panama Basin (7˚51.352’N, 83˚36.418’W at 1364 m
water depth) under the relatively low-salinity waters of thewarm pool in the eastern tropical Pacific. Sediments mostly
consist of hemipelagic clay. Calcareous nannofossils are
the primary biogenic component, exceeding up to 70%(Mix et al., 2003).
Calcareous nannofossils take part in the biogeochemical cycles of the Earth since they play an important role inthe carbon cycle through photosynthesis and calcification
processes (Young, 1994; Baumman et al., 2004). Basedupon quantitative estimations of the absolute abundances
and the species-specific mean coccolith mass, we assess
the paleoproductivity pattern and the temporal distributionof accumulation rates of coccolith-derived carbonate at
ODP Site 1242 in the upper 108.01 mcd (meter composite
depth) which extend back over the past 925 kyr (MIS 22 to1).
The δ18O data on planktonic foraminifera sustain thechronostratigraphic framework (Mix et al., in prep.)
through the past 925 kyr. The overall pattern of paleoproductivity increases downhole, reflecting the gradual rise incoccolith-derived carbonate, especially significant during
the Mid-Brunhes Event (MIS 8 to 15). Paleoproductivity
and accumulation rates of coccolith-derived carbonate also
follow a glacial/interglacial variability, showing maxima
during glacial events. This variability is in agreement withthe typical glacial/interglacial pattern of carbonate production in the Pacific Ocean, previously observed by several
authors (Arrhenius, 1952; Archer, 1991a, b, among others).
Although few intervals of poor preservation obscure thepaleoecological significance of the coccolith carbonate profile, the overall preservation pattern of calcareous nannofossils is good to moderate and supports highpaleoproductivity and accumulation rates of coccolith carbonate during glacials.
References
Archer, D.E. 1991a. Equatorial Pacific calcite preservation cycles: production or dissolution. Paleoceanography, 6: 561–
571.
Archer, D.E. 1991b. Modelling the calcite lysocline. Journal ofGephysical Research, 96: 17037–17050.
Arrhenius, G. 1952. Properties of the sediment and their distribution: Sediment cores from the East Pacific. Swedish DeepSea Expedition 1947-1948, 5: 1-228.
Baumann, K.-H., Böckel, B. & Frenz, M. 2004. Coccolith contribution to South Atlantic carbonate sedimentation. In: H.R.

Thierstein & J.R. Young (Eds). Coccolithophores—from Molecular Processes to Global Impact. Springer-Verlag, Berlin:
367–402.
Mix, A.C., Tiedemann, R., Blum, P. et al. 2003. Proceedings
ODP, Init. Repts., 202. Ocean Drilling Program, College Station, TX. doi:10.2973/odp.proc. ir.202.2003.
Young, J.R. 1994. Functions of coccoliths. In: A. Winter & W.G.
Siesser (Eds). Coccolithophores. Cambridge Univ. Press,
Cambridge: 63–82.

Abstracts

Nutri-thermocline dynamics reconstruction and coccolithcarbonate contribution during the middle and late
Pleistocene in the eastern equatorial Pacific ODP Site 1241
Gatsby-Emperatriz López-Otálvaro, José-Abel Flores, Francisco Javier Sierro
Sediments recovered at Ocean Drilling Program (ODP)
Site 1241, located in the warm pool of the eastern tropical
Pacific (5˚50’N, 86˚26’W at 2027 m water depth), aremostly constituted of clayey foraminiferal-nannofossil
ooze, calcareous nannofossils being the dominant biogenic
component (30-60%; Mix et al., 2003). The sedimentary
sequence studied is controlled by the warm-water regime of
the North Equatorial Countercurrent (NECC), the displacement of the Equatorial Front and the displacement of
the Intertropical Convergence Zone (ITCZ).
A quantitative analysis, taking into account the nannofossil assemblage, the N index (ratio between upper photic
zone species vs. lower photic zone species) and the carbonate-mass produced, allow us to reconstruct the paleoproductivity pattern and the nutri-thermocline variability
over the middle and late Pleistocene. Higher N ratio values reflect high paleoproductivity and an uplifted nutrithermocline, and lower N ratio values indicate low
paleoproductivity and a deep nutri-thermocline. Furthermore, species-specific mean coccolith carbonate mass allowed us to estimate the coccolith carbonate contribution to
the sedimentation at our site, revealing a close relationshipwith the paleoproductivity profile, and thus with the vertical displacement of the nutri-thermocline. Good and moderate preservation of the total coccolith content in thesediments infer that variations in the coccolith carbonate
content responded to variations in the paleo-production of
calcareous nannofossils, rather than dissolution. This strong
relationship suggests maxima of productivity during glacial events, when the ITCZ migrated southward and thewarm-water regime of the NECC was weakened, giving
way to a shoaling of the nutri-thermocline.
Furthermore, the overall pattern of the N ratio reflects
a gradual migration to a more oligotrophic setting during
the past 130 kyr, particularly stressed during Marine Isotope Stage (MIS) 5, suggesting the influence of an El Niñolike setting, as was earlier stated for the eastern tropical
Pacific (Beaufort et al., 2001; López-Otálvaro et al., 2008).
References
Beaufort, L., de Garidel-Thoron, T., Mix, A.C. & Pisias, N.G.
2001. ENSO-like forcing on oceanic primary production during the Late Pleistocene. Science, 293: 2440–2444.
López-Otálvaro, G.-E., Flores, J.-A., Sierro, F.J. & Cachão, I.
2008. Variations in coccolithophorid production in the Eastern Equatorial Pacific at ODP Site 1240 over the last sevenglacial-interglacial cycles. Marine Micropaleontology: doi:
10.1016/j.marmicro.2007.11.009.
Mix, A.C., Tiedemann, R., Blum, P. et al. 2003. Proceedings
ODP, Init. Repts., 202. Ocean Drilling Program, College Station, TX. doi:10.2973/odp.proc.ir.202.2003.

77

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Abstracts

Insight into calcareous nannofossil palaeoecology at the
beginning of the Messinian Salinity Crisis in the classicalsection of Alba (NW Italy)
Francesca Lozar, Simona Cavagna, Pierangelo Clari, Francesco Dela Pierre,
Edoardo Martinetto, Donata Violanti, Andrea Irace, Stefania Trenkwalder
In the last decade, a renewed interest on the onset and developement of the Messinian Salinity Crisis (MSC) led toa general revision of several classic sections in the Mediterranean area (see review in Rouchy & Caruso, 2006). Oneof the classical land Messinian sections, the composite Alba
section of Sturani (1973), has been recently revisited. New
stratigraphical, palaeontological, sedimentological, geochemical and petrographical data were collected in the Tortonian-Messinian sediments cropping out along the Tanaro
River, near Verduno, in order to re-examine the onset anddevelopment of the MSC in this critical area of the Tertiary
Piedmont Basin (BTP).
This work only deals with calcareous nannofossil (CN)data, while integrated biostratigraphical, palaeoecological,
sedimentological and petrographical analyses are in
progress.
The sampled section consists of five main lithologic
units: 1) hemipelagic, laminated marly clay, up to 37 m
thick; 2) three primary selenitic gypsum beds intercalatedwith thinly laminated marly clays (14 m); 3) finely-laminated, fine- to coarse-grained primary ‘balatino’ gypsum(7 m); 4) thinly-bedded marly clays intercalated withcoarse-grained, diagenetic gypsum beds (34 m); 5) marlyclays of the Lago-Mare facies, with root traces; 6) marlyclays of Pliocene age, with abundant marine fossils.
Unit 1 only contains well to moderately preserved CN
assemblages, whose composition reflects the progressive
deterioration of the marine environment prior to the onsetof the MSC (Unit 2).
The occurrence of Messinian marker species, such as
Amaurolithus primus/delicatus, Amaurolithus tricorniculatus identifies the MNN11c subzone of Raffi et al. (2003).
The absence of Nicklithus amplificus, whose occurrence isrestricted to the lower part of the MNN11c subzone, could
indicate the uppermost MNN11c subzone above the LO of
Nicklithus amplificus or, alternatively, could be due to unfavourable palaeoenvironmental conditions. The scatteredoccurrence of Reticulofenestra rotaria, usually recorded
only in MNN11b, may be ascribed to reworking, as
strongly supported by the occurrence of high percentagesof Cretaceous, Paleogene and Early-Middle Miocene CN.
The topmost 3 m of Unit 1 are barren of CN.
The relative abundance of stress-tolerant CN species
supports a pulsating environment with different characteristics of the water column. According to recent studies on
the ecological preferences of several Messinian CN species(Flores et al., 2005; Kowenhoven et al., 2006; Wade &Bown, 2006), we can reconstruct the changes in the environment during the successive phases of the onset of the

MSC. In general, the upper 14 metres of Unit 1 ‘normal’Messinian CN assemblages alternate with several strongly
oligotypic assemblages, with changing composition at different stratigraphic levels. In particular, 12 metres below
the first selenitic gypsum bed, the relative abundance of‘small’ Reticulofenestra (R. minuta and R. haqii combined,
up to 70% of the total assemblage) suggests episodes of eutrophic and brackish-to-hypersaline surface-waters. An
abundance peak of Sphenolithus abies (up to 60% of thetotal assemblage) and high relative abundance of Helicosphaera carteri (up to 20% of the total assemblage) arerecorded 8 metres below Unit 2. The concomitant abundance of both species in our material suggests a shallowwater environment (supported by H. carteri), rich innutrients and with fluctuating, possibly high, salinity. In
fact, S. abies is interpreted as a schizohaline species, and H.
carteri as tolerating high-salinity waters (Kowenhoven etal., 2006). Another peak of ‘small’ Reticulofenestra isrecorded 3 metres below the selenitic gypsum bed, and supports the hypothesis of eutrophic surface-waters, and increasing salinity.
The occurrence of discrete oligotypic CN assemblages,
in a succession of ‘normal’ Messinian CN assemblages,
suggests the presence of surface waters relatively rich innutrients and progressively increasing in salinity towards
the top of Unit 1. The presence of shallow-water markers
supports the idea of a decreasing depth of the basin during
the pre-evaporitic phase, and the development of a progressively restricted environment. The occurrence of ‘normal’ Messinian CN assemblages also testifies that thistrend towards increasing salinity and more restricted environment was interrupted by several episodes of re-establishment of salt concentration close to the global ocean
values during the pre-evaporitic phase.
The occurrence of euryhaline fishes (Aphanius sp.) just
1.5 m below the selenitic gypsum beds of Unit 2 also testifies that the increase in salinity started before the precipitation of gypsum, during the pre-evaporitic phase.
References
Flores, J.-A., Sierro, F.J., Filippelli, G.M., Barcena, M.A., PerezFolgado, M., Vazquez, A. & Utrilla, R. 2005. Surface water
dynamics and phytoplankton communities during depositionof cyclic late Messinian sapropel sequences in the western
Mediterranean. Marine Micropaleontology, 56: 50-79.
Kouwenhoven, T.J., Morigi, C., Negri, A., Giunta, S., Krijgsman,
W. & Rouchy, J.M. 2006. Palaeoenvironmental evolution of
the eastern Mediterranean during the Messinian: constraints
from integrated microfossil data of the Pissouri Basin(Cyprus). Marine Micropalaeontology, 60: 17–44.

Abstracts
Raffi, I., Mozzato, C., Fornaciari, E., Hilgen, F.J. & Rio, D. 2003.
Late Miocene calcareous nannofossil biostratigraphy and astrobiochronology for the Mediterranean region. Micropalaeontology, 49(1): 1-26.
Rouchy, J.M. & Caruso, A. 2006. The Messinian salinity crisis in
the Mediterranean basin: A reassessment of the data and an integrated scenario. Sedimentary Geology, 188-189: 35-67.
Sturani, C. 1973. A fossil eel (Anguilla sp.) from the Messinian ofAlba (Tertiary Piemontese Basin). Palaeoenvironmental andpalaeogeographic implications. In: C.W. Drooger (Ed.).
Messinian events in the Mediterranean. K. Ned. Akad. Wetensch., Amsterdam: 243-255.
Wade, B.S. & Bown, P. 2006. Calcareous nannofossils in extreme
environments: the Messinian Salinity Crisis, Polemi Basin,
Cyprus. Palaeogeography, Palaeoclimatology, Palaeoecology, 233: 271–286.

79

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Abstracts

Calcareous nannofossil, benthic foraminiferal andgeochemical responses to nutrient availability in the SW
Pacific Ocean during the Pleistocene
Claudia Lupi, Iacopo Trattenero, Nicoletta Mancin, Miriam Cobianchi
An integrated micropaleontological (calcareous nannofossils and benthic foraminifera) and geochemical study was
carried out from the IMAGES Site MD97 2114 (eastern
New Zealand, Pacific Ocean), mostly to reconstruct theoceanographic events that occurred in this area during
Pleistocene climate changes. The site studied is locatednorth of the Chatham Rise at a water depth of 1935 meters,
recording the last 1.07 Myr, with substantial continuity of
sedimentation.
Micropaleontological data have been collected using
standard methodologies, then processed by means of themost common and useful statistical methods of mono- andmultivariate analyses. The Principal Component Analysis
applied to relative abundances of the most abundant calcareous nannofossil and benthic foraminiferal species
shows that the distribution patterns of the two groups aremainly driven by nutrient availability controlling primary
productivity.
Calcareous nannofossil data document: up to MIS 18,
the occurrence of a stratified water-column, predominantly
characterised by meso-oligotrophic conditions (e.g., occurrence of Oolithotus fragilis); from MIS 14 to MIS 8, enhanced nutrient levels characterised by high abundance ofGephyrocapsa caribbeanica; finally, from MIS 8 to thecore top, variable trophic conditions. Changes in food supply to the sea floor, related to shallow-water primary productivity, appear to be the main factor controlling benthic
foraminifer distribution. The lower portion of the IMAGES
core, up to MIS 18, is in fact characterized by benthic
foraminifer assemblages indicative of mesotrophic conditions. In the central part of the core, a slow increase in therelative abundances of eutrophic taxa is documented. Then,after a period of re-establishment of mesotrophic conditions (up to MIS 7), a new trend of increasing productivity
characterises the upper part of the core.
The biological events are quite well mirrored by theδ13C curve: the lowermost portion of the core records a predominantly negative δ13C interval, the middle portion (MIS
15-8) is characterised by heavier values of the δ13C, and finally, after an interval of re-established negative values,
several positive peaks are documented up to the MIS 4.

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81

Calcareous nannofossil biostratigraphy of the Sarcheshmeh
and Sanganeh Formations from the Takal Kuh section,
Kopet Dagh Basin (NE Iran)
Azam Mahanipour, Anoshiravan L. Kani, Naser Raisossadat
The Sarcheshmeh and Sanganeh Formations are widelydistributed in the Iranian part of the Kopet Dagh Basin, extending from east to west. The present study concentrates
on calcareous nannofossil content of a relatively poorly
studied sequence of the Sarcheshmeh and Sanganeh Formations, which is located in the Takal Kuh section in thewestern part of the basin. The section measures about 1600
meters and consists of marl, limestone, marly limestoneand shale. The distribution of the nannofloral assemblagesof the Sarcheshmeh and Sanganeh sediments reveal thepresence of Zones CC6 and CC7 of Sissingh (1977) indicating an Upper Barremian-Upper Aptian age that is wellcorrelated with the ammonites zonation in the lower parts.
Nannoconids are present throughout the section, butreach their maximum abundance in the upper parts, thus indicating warm, nutrient-depleted surface waters for the environment of deposition (Erba, 1994).
References
Sissingh, W. 1977. Biostratigraphy of Cretaceous calcareous
nannoplankton. Geol. Mijnbouw, 56: 37-65.
Erba, E. 1994. Nannofossils and superplumes: The early Aptian‘nannoconid crisis’. Paleoceanography, 9: 483- 501.

82

Abstracts

MIS11 calcareous nannoplankton assemblages off western
Iberia (MD01-2443): Paleoecological andpaleoceanographic implications
Sara Marreco, Mário Cachão, Lúcia de Abreu, Vanda Brotas
Orbital parameters and greenhouse gas concentrations during Marine Isotope Stage (MIS) 11 (428 - 360 ka) are mostsimilar to the Holocene, and thus MIS11 is considered apast analogue of the present day interglacial climatic system. For this study, a high-resolution set of 216 samples
for a 61 kyr time-interval from the MIS 11 section of thecore MD01 – 2443 (western Iberian margin; de Abreu etal., 2005) was analysed.
The main kenotic affinity associations of calcareous
nannoplankton were identified and characterized by establishing possible linear correlations between certain coccolithophores and paleoecological and/or paleoclimatic
proxies. Thus, possible paleoenvironmental and paleoproductivity forcing mechanisms are addressed by statisticallymatching our time-series against other micropaleontological (benthic and planktonic foraminifera) and geochemical(δ18O) proxies from de Abreu et al. (2005). Results will bepresented and discussed, namely the possible existence of
sub-Milankovitch cycles through the identification of
meaningful frequencies for each taxon.
Referencede Abreu, L., Abrantes, F., Shackleton, N.J., Tzedakis, P., McManus, J., Oppo, D. & Hall, M. 2005. Ocean climate variability in the eastern North Atlantic during interglacial marine
isotope stage 11: A partial analogue to the Holocene. Paleoceanography, 20: 1-15.

Abstracts

Nannofossil biostratigraphy of Miocene sections in two
wells from the Gulf of Suez, Egypt
Akmal M. Marzouk
Calcareous nannofossils were studied in Miocene sediments (Early-Middle Miocene) of two wells (Gulf of Suez,
Egypt). One of them is located in the extreme northern partof the Gulf of Suez (Darag 17-1A), at a latitude of 29˚30’,
and the second one (GS 148-1) is at a latitude of 29˚ (in thecenter of the Gulf of Suez). In the two studied sections, theabundance fluctuations of some nannofossil marker-species
proved to be a very useful tool for correlation. However,
the index species of calcareous nannofossils is not abundant, but common to few and continuous in the subsurface
wells of the Miocene of the Gulf of Suez. The quantity ofindex species was determined by means of quantitative
methods in order to test the reliability of biohorizons usedin the recent literature dealing with a Mediterranean Neogene Nannoplankton Zonation (MNN1-6) (Fornaciari &Rio, 1996; Fornaciari et al., 1996). Some problems linked
to stratigraphical boundaries through the Miocene are discussed, as well as some peculiarities of the Mediterranean
calcareous nannofossil assemblages.
In the Middle Miocene sediments of the uppermost
Rudeis, Kareem and Belayim Formations, calcareous nannofossils were not recorded in the northern part of the Gulf
of Suez (Darag 17-1A) well, while they were deposited in
the GS (148-1) well, which is located relatively southwards. The partial absence of the uppermost Rudeis, Kareem and Belayim nannofloral assemblages from theextreme northern part of the Gulf of Suez (Darag 17-1A)
well, including zones MNN4, MNN5 and MNN6a, may be
due to unfavorable environmental conditions that prevailed
at the end of the deposition of the upper Rudeis Formation.
This absence may also be related to tectonic movements,
which caused an unconformity within the Rudeis Formation, likely related to an uplift of the northern part of the
Gulf of Suez area. Due to the presence of most common
helicoliths in the assemblage, the uppermost part of theDarag 17-1A well was referred to shallower-water, nearshore conditions. Moreover, the extremely thin Kareem
section, and the lack of thick evaporites, in the northernpart of the Gulf of Suez Darag 17-1A well, indicates a period of no subsidence and low deposition in the Middle
Miocene.

83

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Thoracospheres: the evolution of calcification in
dinoflagellates
Sebastian Meier
Calcification has evolved multiple times in many different
branches of the eukaryotic part of the tree of life, and also
one small sprig within the dinoflagellates has acquired thischaracter during its evolution. The timing of this event haslong been unclear, as some isolated records of microfossils
with morphological characters attributed to the calcareous
dinoflagellates, so-called calcispheres, are known from theUpper Triassic, whereas an uninterrupted record of undoubted calcareous dinoflagellates exists only since theUpper Jurassic. Molecular clock calculations with alternative calibration points for the origin of calcareous dinoflagellates indicate that a Jurassic origin is more likely than a
Triassic one (Gottschling et al., 2008). This is in good
agreement with traditional morphological dinoflagellatetaxonomy, as the Triassic calcispheres show no indicationof tabulation, whereas the true calcdino tabulation is remarkably stable over their evolutionary history.
A major discrepancy between molecular and morphological classifications lies in the current concept of classifying calcareous dinoflagellates by the crystallographic
orientation of the crystals within the wall. Calcification in
calcdinos has evolved first in the diploid life-cycle phase,and the majority of species investigated today forms
diploid calcareous cysts. Diploid calcification was lost in a
subclade of the calcareous dinoflagellates in which the haploid life-cycle phase has diversified. Calcification was regained secondarily in two genera of this clade, and thevegetative calcareous coccoid cells are the dominant lifecycle phase. Therefore, one part of the taxonomic confusion in calcareous dinoflagellates seems to result fromcomparing non-homologous calcareous structures, i.e.
diploid resting cysts and vegetative coccoid cells (Meier etal., 2007).
Reinvestigating the ultrastructure of the calcareous
walls in calcdinos is therefore urgently needed for a better
understanding of unifying molecular, morphological andfossil phylogenies. First results show that the three major
clades in calcareous dinoflagellates may be represented
also by three different biomineralisation modes. Unfortunately, the underlying biogeochemical processes are largely
unknown. There are now first studies on the isotope chemistry of the calcareous wall of dinoflagellates representing
different proposed biomineralisation modes, and all ofthem show a characteristic strong depletion in δ13C against
equilibrium conditions in modern and fossil species(Friedrich & Meier, 2003; Minoletti et al., 2004; Zonneveld
et al., 2007), indicating highly specialized biomineralisation pathways in calcareous dinoflagellates that are maintained despite the evolution of different modes of
biomineralisation.

References
Friedrich, O. & Meier, K.J.S. 2003. Stable isotopic indication forthe cyst formation depth of Campanian/Maastrichtian calcareous dinoflagellates. Micropaleontology, 49: 375-380.
Gottschling, M., Renner, S., Meier, K.J.S., Keupp, H. & Willems,
H. 2008. Timing deep divergence events in calcareous dinoflagellates. Journal of Phycology, 44: 429-438.
Meier, K.J.S., Young, J.R., Kirsch, M. & Feist-Burkhardt, S. 2007.
Evolution of different life-cycle strategies in oceanic calcareous dinoflagellates. European Journal of Phycology, 42: 8189.
Minoletti, F., de Rafelis, M., Renard, M., Gardin, S. & Young, J.
2005. Changes in the pelagic fine fraction carbonate sedimentation during the Cretaceous-Paleocene transition: contribution of the separation technique to the study of Bidart
section. Palaeogeography, Palaeoclimatology, Palaeoecology, 216: 119-137.
Zonneveld, K.A.F., Mackensen, A. & Baumann, K.-H. 2007. Stable oxygen isotopes of Thoracosphaera heimii (Dinophyceae)
in relationship to temperature; a culture experiment. Marine
Micropaleontology, 64: 80-90.

Abstracts

85

Response of coccolithophores to atmospheric andoceanographic changes during the Holocene African Humid
Period in the East Atlantic, NW Africa
Alejandra Mejía-Molina, José-Abel Flores, Francisco Javier Sierro, M. Ángeles
Barcena, Francis Grousset, Elsa Jullien
Core MD03-2705 -DUST was recovered on a seamount at
18˚05’N and 21˚09’W at a water depth of 3085 m off Mauritania-Senegal (NW Africa) during the R/V Marion
Dufresne II Cruise (PICABIA, summer/fall 2003). The
continuous sediment sequence consists of foraminifer andnannofossil oozes. The age-model is based on the correlation of δ18O record of the benthic foraminifer Cibicides
wuellerstorfii to the SPECMAP and ODP Hole 658C
records (Martinson et al., 1987; deMenocal et al., 2000).
Additionally, these results were compared to 14C analyses.
Qualitative analyses, carried out on coccolithophores together with wind-transported microfossils (phytholiths andfresh-water diatoms) from continental NW African areas,
allow us to interpret variations in the direction and intensityof winds and their relationship with superficial oceanographic dynamics during 14.5-5.5 ka cal. BP, associatedwith the African Humid Period (Sarnthein et al., 1982; deMenocal et al., 2000). The terrigenous record exhibits awell-defined period of low influx associated with the
African Humid Period (AHP), when the Sahara was nearlycompletely covered by vegetation and supporting perennial lakes. This period has been attributed to a strengthening of the African monsoon, due to gradual orbital increases
in summer insolation. Variations in the surface-water productivity of coccolithophores (variations in the nutricline/thermocline position) were monitored using the N
ratio between Noelaerhabdaceae (inhabitants of the upper
photic zone) versus Florisphaera profunda (a lower photic
zone inhabitant). High values in the N ratio imply a relatively high nutricline/thermocline position. During the
AHP, the high productivity conditions are related with highvalues in the N ratio with abundant specimens of Noelaerhabdaceae. The transition between the Younger Dryas andthe Holocene is interpreted as a rapid shift to arid conditions. The end of this period is coincident with high abundance in fresh-water diatoms and phytholiths, and with aprogressing positive pulse in the Ti/Al ratio, suggesting intensification in the wind regime. At this time, the coccolithophore assemblage shows a dramatic decrease in the
cool-water species Gephyrocapsa muellerae, interpreted asa return to warmer conditions.
References
deMenocal, P., Ortiz, J., Guilderson, T., Adkins, J., Sarnthein, M.,
Baker, L. & Yarusinsky, M. 2000. Abrupt onset and termination of the African Humid Period: rapid climate responses togradual insolation forcing. Quaternary Science Review, 19:347-361.
Martinson, D.G., Pisias, N.G., Hays, J.D., Imbrie, J., Moore, T.C.
& Shackleton, N.J. 1987. Age dating and the orbital theory of

the Ice Ages: development of a high-resolution 0 to 300, 000year chronostratigraphy. Quaternary Research, 27: 1-29.
Sarnthein, M., Thiede., J., Pflaumann, U., Erlenkeuser, H.,
Fütterer, D., Koopmann, B., Lange, H. & Seibol, E. 1982. Atmospheric and oceanic circulation patterns off Northwest
Africa during the past 25 million years. In: U. Rad, I. Hinz, M.
Sarnthein & E. Scibol (Eds). Geology of the Northwest Africa
continental margin. Springer-Verlag, New York: 547-604.

86

Abstracts

Coccolithophore assemblages of the Early-Middle Miocene in
the Colombian Caribbean Sea: A correlation between the
Arroyo Alférez section and ODP Leg 165, Site 999
Alejandra Mejía-Molina, José-Abel Flores, Vladimir Torres Torres, Francisco
Javier Sierro
Correlating onshore sequences and offshore-cored sections
is often critical to develop an integrated biostratigraphic
model. Here, we examine high-resolution records fromODP Leg 165, Site 999 in concert with an onshore section,
Arroyo Alférez, from Colombia. We used the standard biozonations proposed by Martini (1971) and Bukry (1973,1975) for detailed Miocene biostratigraphy. Those biozonations were established in detailed sequences from the
Caribbean Sea. The base of the onshore Arroyo Alférez sequence studied here is lower Oligocene NP23 (CP18) toMiddle Miocene NN5 (CN4), and provides a continuousrecord and an excellent preservation of coccolithophore assemblages. The analyses carried out from samples, collected from a core of ODP Site 999 in the Colombian
Basin, covers a continuous Miocene-Pleistocene interval,
revealing an irregular and intermediate preservation of thecoccolithophore record. The most representative taxa identified in the interval studied are Cyclicargolithus floridanus, Cyclicargolithus abisectus, Reticulofenestra minuta,
Reticulofenestra minutula, Reticulofenestra pseudoumbilicus and Sphenolithus moriformis. We note also that Helicosphaera spp. was abundant in some intervals, while
discoasterids increase towards the top of the sections. Mostof the classical biostratigraphic events have been identified
in both sequences. The study of the Arroyo Alférez onshore
sequence constitutes the first biostratigraphic scheme based
upon calcareous nannofossils. This scheme provides abiochronologic frame for the Cenozoic of northern Colombia, which has direct applications for oil exploration in theoffshore areas of the Colombian Caribbean Basin. Its correlation with the well-calibrated ODP Site 999 offshore
record provides a robust biostratigraphic framework andrepresents a potential key for future paleoceanographic interpretations.
References
Bukry, D. 1973. Coccolith and silicoflagellate stratigraphy, Tasman Sea and Southern Pacific Ocean, Deep Sea Drilling Project Leg 21. Initial Reports of the Deep Sea Drilling Project,
21: 885-893.
Bukry, D. 1975. Coccolith and silicoflagellate stratigraphy, northwestern Pacific Ocean, Deep Sea Drilling Project, Leg 32.
Initial Reports of the Deep Sea Drilling Project, 32: 677-701.
Martini, E. 1971. Standard Tertiary and Quaternary calcareous
nannoplankton zonation. In: A. Farinacci (Ed.). Proceedingsof the II Planktonic Conference, Roma, 1970, 2: 739-785.

Abstracts

87

Calcareous nannofossil extinction pattern across theCretaceous/Tertiary boundary in the Tethyan Realm
Mihaela C. Melinte-Dobrinescu, Marcos A. Lamolda, Ana-Voica Bojar
This paper presents detailed calcareous nannofossil investigations carried out across the K/T boundary interval insections from the Tethyan Realm (Caravaca from the Betic
Cordilleras, SE Spain, and Pietroşiţa from the southern partof the Eastern Carpathians, Romania). The Caravaca section was the object of one of the first detailed calcareous
nannoplankton investigations for the K/T boundary interval(Romein, 1977), as well as of more recent micropaleontological (foraminiferal and nannofloral) and isotope studies(Kaiho & Lamolda, 1999; Lamolda et al., 2005). In the
Pietroşiţa section, isotope measurements and fluctuations
were recently published (Bojar et al., accepted).
In the studied sections, calcareous nannofossil events
are similar to those recorded everywhere in the Tethyan
Realm across the K/T boundary (Aguado, 1993; Pospichal,
1995; Melinte, 1999; Gardin, 2002; Tantawy, 2003, among
many others). Namely, the successive first occurrences(FOs) of Micula murus, Nephrolithus frequens and M. prinsii, followed by the extinction of most Cretaceous nannoplankton, as well as by ‘blooms’ of the calcareous
dinoflagellate Thoracosphaera operculata and of the nannofossil Braarudosphaera bigelowii.
The oldest observed step in the decline of Upper Cretaceous nannofloras, both in terms of species richness(number of taxa per sample) and abundance (number of
specimens per field of view), was identified in the Spanish
and Romanian sections below the ‘fallout’ lamina of theK/T boundary, above the FO of M. prinsii. This decline isexpressed by a decrease of 15-20% in species richness andup to 30% in abundance. Taking into account the sedimentation rate for each investigated section, the first nannofloral decline took place around 4.5 kyr prior to the K/T event.
A second nannofloral decline (approximately 2 kyr prior to
the K/T event) is recorded in the two studied sections, andis marked by an abundance decrease of 60-70%, while
species richness has no relevant changes. We may assume
that these two Upper Maastrichtian steps in nannofloral decline observed in both Tethyan sections mirror paleoenvironmental changes that took place contemporaneously inthe two investigated regions, and therefore indicate a stepwise extinction. Alternatively, this pattern may be an artifact of preservation and/or of local palaeoecologicalconditions (the Signor-Lipps effect, a false extinction) reported also by Gardin (2002) around the K/T boundary atElles, Tunisia.
At the K/T boundary, around 80% of Cretaceous nannofossils disappeared. The survivors (Cretaceous taxa
which are believed to cross the K/T boundary, having aconsistent and continuous occurrence in the Tertiary nannofossil assemblages) are B. bigelowii, B. alta, Chiastozygus ultimus, Cyclagelosphaera reinhardtii, Markaliusinversus, Neocrepidolithus neocrassus, Octolithus multi-

plus and Zeugrhabdotus sigmoides. In both the studied sections, Biantholithus sparsus sporadically occurs from the
topmost Maastrichtian.
Just above the K/T boundary (the Ir ‘layer’), T. operculata significantly increases in abundance from 0.5% up
to 5% and a ‘bloom’ of Markalius inversus occurred. The
dominant components of the basal Paleocene nannofloral
assemblages are Watznaueria barnesiae and Micula decussata, which together account for up to 80% of the totalnannofloras. Notably, both taxa are the dominant components of Upper Maastrichtian nannofloras, representing together around 40-50% of the total assemblage, but theyshow a continuous decrease towards the top of the analyzed
sections (in the lowermost Paleocene).
Within the basal Paleocene of the Spanish and Romanian sections, successive ‘blooms’ of T. operculata (up to60%) and B. bigelowii (up to 25-30%) were observed. The
isotope data show a negative correlation with the Thoracosphaera ‘blooms’ and a positive correlation with the B.
bigelowii ‘bloom’ in the Romanian succession.
References
Aguado, R. 1993. Nanofósiles del Cretácico de la Cordillera
Bética, Bioestratigrafía. Unpubl. PhD thesis, Universidad deGranada: 413pp.
Bojar, A.V., Melinte, M.C. & Bojar, H.P. Accepted. A continuous
Cretaceous/Paleogene red bed section in the Romanian
Carpathians. SEPM Special Publication.
Gardin, S. 2002. Late Maastrichtian to early Danian calcareous
nannofossils at Elles (Northwest Tunisia). A tale of one million years across the K-T Boundary. Palaeogeography,
Palaeoclimatology, Palaeoecology, 178: 211-231.
Kaiho, M.A.& Lamolda, M.A. 1999. Catastrophic extinction ofplanktonic foraminifera at the Cretaceous/Tertiary boundary
evidenced by stable isotopes and foraminiferal abundance at
Caravaca, Spain. Geology, 27(4): 355-358.
Lamolda, M.A., Melinte, M.C. & Kaiho, K. 2005. Nannofloral
extinction and survivorship across the K/T boundary at Caravaca, southeastern Spain. Palaeogeography, Palaeoclimatology, Palaeoecology, 224: 27-52.
Melinte, M.C. 1999. Cretaceous/Tertiary Boundary in the East
Carpathians (Romania) based on nannofloral evidence. Acta
Paleontologica Rumaniae, II: 269-273.
Pospichal, J.J. 1995. Cretaceous/Tertiary boundary calcareous
nannofossils from Agost, Spain. In: J.-A. Flores & F.J. Sierro(Eds). Proceedings of the 5th INA Conference, Salamanca:
185-217.
Romein, A.J.T. 1977. Calcareous nannofossils from the Cretaceous/Tertiary boundary interval in the Barranco del Gredero(Caravaca, Prov. Murcia, SE Spain). Proceedings of the Kon.
Ned. Akad. van Wetensch., Amsterdam, B80(4): 256-279.
Tantawy, A.A.A.M. 2003. Calcareous nannofossil biostratigraphy
and paleocecology of the Cretaceous-Tertiary transition in thecentral eastern desert of Egypt. Marine Micropaleontology,
47: 323-356.

88

Abstracts

Reconstruction of the interregional Late Cretaceous
sea-level record using nannofossil biostratigraphy
Svetlana F. Mizintseva
Biostratigraphy is a powerful tool in many different areasof stratigraphic reconstructions. Nannofossil biostratigraphy is an indispensable tool for a variety of stratigraphic
work in many different regions. My studies have focusedon the application of nannofossils biostratigraphy to Late
Cretaceous sea-level reconstructions in the northern part of
the Atlantic passive margin-New Jersey coastal plain. My
approach has been to integrate sequence stratigraphy, paleobathymetry and biostratigraphy to derive a record of
Late Cretaceous sea-level changes in the New Jersey
coastal plain and establish firm biostratigraphy for interregional reconstructions. Use of calcareous nannoplankton
biostratigraphy allows resolving the ages of the Santonian–Campanian sequences of New Jersey coastal plain. The

ages are from 78.8 to 84.5 Ma and they correspond to CC16
(MeI sequence), CC17-18 (MeII sequence), CC18-19(MeIII sequence) zone of calcareous nannoplankton biozonation of Sissingh (1977) and Perch-Nielsen (1985). The
following markers are found on New Jersey coastal plain:
the lowest occurrence (LO) of Lucianorhabdus cayeuxii
identifies the base of Zone CC16, the LO of Calculites obscurus and the presence of Calculites ovalis identifies thebase of Zone CC17, the LO of Broinsonia parca parca
identifies the base of Zone CC18, and the highest occurrence (HO) of Marthasterites furcatus identifies the baseof Zone CC19 (Fig 1).
This work provides a great potential for interregional
sea-level reconstructions and evaluation of eustasy as apossible mechanism for New Jersey
coastal plain sea-level changes. My future work is directed on interregionalcorrelation of the Santonian–Campanian strata using nannofossils biostratigraphy.
Reference
Perch-Nielsen, K. 1985. Mesozoic calcareous nannofossils. In: H.M. Bolli, K.
Perch-Nielsen & J.B. Saunders (Eds).
Plankton stratigraphy. Cambridge University Press, Cambridge: 427-554.
Sissingh, W. 1978. Biostratigraphy of Cretaceous calcareous nannoplankton. Geologie en Mijnbouw, 57: 433-440.

All figured specimens are from the Millville, NJ
corehole. Depths refer to the sample from which
the figured specimen was taken. All speciesnames follow Sissingh (1978) and Perch-Nielsen(1985). XPL = cross-polarized light, NL- normal
light. a-c) Broinsonia parca parca (1228ft;
374.2m): a) XPL 0˚ rotated, b) XPL 45˚ rotated,c) NL. d-f) Calculites ovalis (1236ft; 376.7m): d)
XPL 0˚ rotated, e) XPL 45˚ rotated, f) NL. g-i)
Calculites obscurus (1251ft; 381.3m): g) XPL 0˚
rotated, h) XPL 45˚ rotated, i) NL; j-l) Marthasterites furcatus (1221ft; 372.1m): j) XPL 0˚ rotated, k) NL, l) NL; m-o) Lucianorhabdus
cayeuxii (1251ft; 381.3m): m) XPL 0˚ rotated, n)
XPL 45˚ rotated, o) NL

Abstracts

89

New high-resolution calcareous nannofossil biostratigraphy
and Fasciculithus evolutionary trend across the DanianSelandian transition at ODP Site 1262, comparison with
Zumaia (Spain) and the Qreiya (Egypt) sections
Simonetta Monechi, Viviana Reale, Gilen Bernaola, Barbara Balestra
High-resolution calcareous nannofossil analysis has been
carried out on an expanded and continuous Paleocene sequence recovered during Leg 208 (Walvis Ridge, South Atlantic) at Site 1262. The detailed magnetostratigraphy andastronocyclostratigraphy of Westerhold et al. (2008) haveallowed a precise calibration of the recognized bio-events.
Twenty meters of the composite section across the nannofossil Zones NP4-NP5 have been studied in order to define
the lowest occurrence (LO) of Fasciculithus, and the evolutionary trend of this genus until the LO of Fasciculithus
tympaniformis.
The first specimens of Fasciculithus (F. magnicordis
and F. magnus) have been observed in the middle part ofChron C27r, just above the LO of Toweius pertusus, andprior to the LO of the genus Sphenolithus (in agreementwith Agnini et al., 2007). The distribution and abundanceof Fasciculithus vary throughout the studied interval, anddiaplay two radiation intervals. The first radiation of Fasciculithus, that involves the occurrence of F. chowii and related species, is recorded in the upper part of Chron C27n.
The second one, characterized by the assemblage of F. ulii
gr. and F. janii gr., occurs in the lower part of Chron 26r.
The distribution of Fasciculithus is not continuous; in fact,
between the two radiations, an interval barren of Fasciculithus has been detected. The LO of F. tympaniformis has
been observed in the upper part of Chron C26r between the
LO of Neochiastozygus perfectus and the LO of Toweius
eminens.
A taxonomic review of the early species of Fasciculithus, and the detailed stratigraphic distribution of thesetaxa, have permitted the identification of new species andsuggested a possible evolutionary trend. The succession of
the events recognized at Site 1262 confirms the bio-events
documented in the Zumaia section, proposed as stratotype(GSSP) of the Danian/Selandian boundary (Bernaola et al.,2008). In general, the observations made at the Qreiya section validate the succession of the events recognized by Rodriguez & Aubry (2006) in the same section, even if someinconsistencies have been observed, mainly related to thedifferent taxonomic concept of a few Fasciculithus species.
References
Agnini, C., Fornaciari, E., Raffi, I., Rio, D., Röhl, U. &Westerhold, T. 2007. High-resolution nannofossil
biochronology of middle Paleocene to early Eocene at ODP
Site 1262: Implications for calcareous nannoplankton
evolution, Marine Micropaleontology, 64: 215–248. doi:
10.1016/j.marmicro.2007.05.003
Bernaola, G., Martín-Rubio, M. & Baceta, J.I. In press. New highresolution calcareous nannofossil analysis across the Danian-Selandian transition at the Zumaia section: comparisons with
South Tethys and Danish sections. Geologica Acta.
Rodriguez, O. & Aubry, M-P. 2006. Lower to Middle (DanianSelandian) Paleocene calcareous nannofossil stratigraphy of
the Qreiya section (Egypt) In: F. Caballero et al. (Eds). Climate and Biota of the Early Paleogene, 2006, abstracts. Bilbao: 111.
Westerhold, T., Röhl, U., Raffi, I., Fornaciari, E., Monechi, S.,
Reale, V., Bowles J. & Evans, H.F. 2008. Astronomical calibration of the Paleocene time. Palaeogeography, Palaeoclimatology, Palaeoecology, 257: 377-403.

90

Abstracts

Sea-surface dynamics and coccolithophore behaviour duringsapropel deposition of Marine Isotope Stages 7, 6 and 5 in
the western Adriatic SeaÁurea Narciso, José-Abel Flores, Mário Cachão, Francisco Javier Sierro, Elena
Colmenero-Hidalgo, Andrea Piva, Alessandra Asioli
A detailed calcareous nannofossil analysis was performed
on 234 samples from the core PRAD1-2, collected in the
Mid-Adriatic Deep during the PROMESS1 Cruise. The selected sequence includes the Marine Isotope Stages 7, 6
and 5, crossing several sapropel layers (S8 to S3) (Piva etal., 2008). The main goal of the present study was to recognise changes in calcareous nannopankton distribution pattern during MIS 7, 6 and 5, and in particular across theassociated sapropel layers.
Most of the sedimentological, geochemical and micropaleontological studies (e.g. Capozzi & Picotti, 2003;
Arnaboldi & Meyers, 2003; Rio et al., 1997) refer that
sapropels are dark-coloured organic-rich layers interbedded in the normal pelagic sediments of the Mediterranean
Sea. They are related to climatic or oceanographic variations. Sapropel generation is also associated to orbital scale
oscillations under conditions of maximum summer insolation, corresponding to a minimum of the precession component of Earth’s orbit, with a periodicity of 21kyr (Hilgen,
1991; Lourens et al., 1996; Hilgen et al., 1997).
The results of this work indicate a decrease of the total
coccolith abundance during most of the sapropels. A similar pattern was previously observed in others sectors of theMediterranean (e.g., Negri &Villa, 2000; Negri & Giunta,
2001), while the reworked nannoliths exhibit an opposite
pattern. The analysis of single species (namely, C. pelagicus, H. carteri, Syracosphaera spp., R. clavigera+Calciosolenia spp., B. bigelowii and small taxa) shows adecrease in abundance during MIS 7, while during MIS 6
and 5 the opposite pattern occurs. Another important feature of the studied samples is the significant increases in
Coccolithus pelagicus and in Helicosphaera carteri at the
beginning of MIS 7 sapropel layers, reflecting a phase characterized by cold and mixed waters (eutrophication). However, the same pattern is not so evident for the otherinterglacial stage (MIS 5). Our results also show important
increments of Syracosphaera, Rhabdosphaera+Calciosolenia, and Braarudosphaera at the top or above theend of the sapropels; these increments are clearer for MIS
5. This phase is consistent with the end of dryer and cold
conditions, and subsequent reestablishment of the generaloligotrophy of surface waters. During MIS 7, between
these phases and during most of the sapropel deposition,
increases in reworked taxa are observed that reflect a more
intense runoff. The consequences of this important fluvial
erosion may have hampered the development of autochthonous species.
In general, our results indicate the existence of fluctuations in the calcareous nannofossil content between theinterglacial stages 7 and 5, and also between these two andthe glacial stage 6, revealing a transition of different paleoceanographic conditions across the analysed interval. A
similarity in the environmental conditions occurring during sapropel deposition of each stage was also detected.
References
Arnaboldi, M. & Meyers, P. 2003. Geochemical evidence for paleoclimatic variations during deposition of two Late Pliocene
sapropels from the Vrica section, Calabria. Palaeogeography,
Palaeoclimatology, Palaeoecology, 190: 257-271.
Capozzi, R. & Picotti, V. 2003. Pliocene sequence stratigraphy,
climatic trends and sapropel formation in the Northern Apennines (Italy). Palaeogeography, Palaeoclimatology, Palaeoecology, 190: 349-371.
Hilgen, F.J. 1991. Astronomical calibration of Gauss to Matuyama
sapropels in the Mediterranean and implication for the Geomagnetic Polarity Time Scale. Earth Planetary Science Letters, 104: 226-244.
Hilgen, F.J., Krijgsman, W., Langereis, C.G. & Lourens, L.J.
1997. Breakthrough made in dating of the geological record.
EOS, Trans.-Am. Geophys. Union, 78: 286-289.
Lourens, L., Antonarakou, A., Hilgen, F.J., Van Hoof, A.A.M.,
Vergnaud Grazzini, C. & Zachariasse, W.J. 1996. Evaluationof the Plio-Pleistocene astronomical timescale. Paleoceanography, 11: 391-413.
Negri, A. & Giunta, S. 2001. Calcareous nannofossil paleoecology in the sapropel S1 of the eastern Ionian sea: paleoceanography
implications.
Palaeogeography,
Palaeoclimatology, Palaeoecology, 169: 101-112.
Negri, A. & Villa, G. 2000. Calcareous nannofossil biostratigraphy,
biochronology
andpaleoecologyattheTortonian/Messinian boundary of the Faneromeni section(Crete). Palaeogeography, Palaeoclimatology, Palaeoecology, 156: 195-209.
Piva, A., Asioli, A., Schneider, R., Trincardi, F., Andersen, N.,
Colmenero-Hidalgo, E., Dennielou, B., Flores, J.-A. &Vigliotti, L. 2008. Climatic cycles as expressed in sedimentsof the PROMESS1 borehole PRAD1-2, central Adriatic, forthe last 370ka: 1. Integrated stratigraphy. Geochem., Geophys., Geosyst., 9: 1-21.
Rio, D., Channell, J., Bertoldi, R., Poli, M., Vergerio, P., Raffi, I.,
Srovieri, R. & Thunell, R. 1997. Pliocene sapropels in thenorthern Adriatic area: chronology and paleoenvironmental
significance. Palaeogeography, Palaeoclimatology, Palaeoecology, 135: 1-25.

Abstracts

91

Late Eocene-Late Oligocene nannofossil paleoecology at
Site 1090 (Agulhas Ridge, South Atlantic)
Laura Pea, Chiara Fioroni, Davide Persico, Silvia Palandri, Giuliana Villa
Climate changes occurred between the Paleogene and the
Neogene, marking the transition between Greenhouse to
Icehouse conditions. The Paleogene time is characterized
by a general cooling trend, culminating in the Early
Oligocene Oi-1 event (~ 33.5 Ma) (Miller et al., 1991; Zachos et al., 1996; Lear et al., 2000; Zachos et al., 2001).
This trend is actually punctuated by several short warming
phases, recorded by foraminifera carbon and oxygen isotopes (Kennet & Stott, 1990; Zachos et al., 2001; Bohaty &Zachos, 2003), and by nannofossil communities at several
high-latitude (Bralower, 2002; Persico & Villa, 2004; Villa& Persico, 2006; Villa et al., subm.) and mid-latitude sites(Agnini et al., 2006; Gibbs et al., 2006). The Late Eoceneshows a strong climatic instability, with periodicity ofwarming and cooling phases. The Eocene/Oligocene
boundary and the next Oi-1 event represent the most abrupt
climatic change, followed by a long, cool period spanningmost of the Oligocene.
A paleoecological study of the nannofossil assemblages
has been carried out at Hole 1090B, based on a quantitative
analysis of high-resolution samples. The studied intervalspans from the Late Eocene to the Late Oligocene. This
Hole is located on the southern flank of the Agulhas Ridgeon the Subantarctic sector of the Atlantic Ocean (42˚54’S).
It lies along the boundary between the North Atlantic Deep
Water and the Circumpolar Deep Water. Thanks to its position above the Carbonate Compensation Depth (3702 m),
the nannofossil assemblage preservation is from poor togood in most of the section, even thought some intervals
are barren. A well-preserved magnetostratigraphic signal
through all of the section, and nannofossil biostratigraphy,
provided the time framework essential for interpreting theassemblage variations.
Methodology used in previous works (Persico & Villa,
2004; Villa et al., subm.) were applied here to the dataset
to obtain the total abundance and the Shannon–Weaver
species diversity index; furthermore, for each species,
abundance curves were plotted as percentages, and also Rmode principal component analysis (PCA), and R-mode
cluster analysis were performed. PCA, allowed us to identify the major components of the nannofossil assemblage,
and to plot the factors that explain the maximum variance,
here interpreted in a paleoecological view.
Once compared, the results derived from the two methods allowed us to obtain a paleoecological classification of
the nannofossil assemblages, interpreted in terms of paleoecological changes (cool, temperate, and warm-watertaxa). Using this classification, we identified abundancechanges of each specific group of taxa, here interpreted
mainly as related to sea-surface temperature variations. Importantly, the Oi-1 cooling event, previously recognized inother Southern Ocean sites as occurring just after the

Eocene-Oligocene boundary, has been identified at about
257 mcd. This datum reinforces the position of the epoch
boundary proposed by Channell et al. (2003), on the basisof the magnetostratigraphy, rather than the boundary proposed on the basis of foraminifer biostratigraphy.
The results obtained in this study are compared withdata from some Southern Ocean sites (689, 738, 744, 748)
(Persico & Villa, 2004; Villa & Persico, 2006; Villa et al.,subm.), in order to obtain an ideal latitudinal transect along
the Indian and Atlantic oceans. Compared to southernmost
locations, at Site 1090, warm-water taxa are more abundant and temperate-water taxa have a more constant pattern; this is plausibly linked to the lower-latitude positionof this site, north of the subantarctic front, where temperate forms thrive and are less affected by climatic changes.
As it is shown here, as well as in numerous, previous
studies from different areas, nannofossils resulted to be
useful tools for paleoclimatic and paleoceanographic reconstructions.
References
Agnini, C., Fornaciari, E., Rio, D., Tateo, F., Backman, J. &Giusberti, L. 2006. Responses of calcareous nannofossil assemblages, mineralogy and geochemistry to the environmental perturbations across the Paleocene/Eocene boundary in the
Venetian Pre-Alps. Marine Micropaleontology, 63: 19-38.
doi:10.1016/j.marmicro.2006.10.002.
Bohaty, S.M. & Zachos, J.C. 2003. Significant Southern Ocean
warming event in the late middle Eocene. Geology, 31: 10171020.
Bralower, T.J. 2002. Evidence of surface water oligotrophy during the Paleocene–Eocene thermal maximum: nannofossil assemblage data from Ocean Drilling Program Site 690, MaudRise, Weddell Sea. Paleoceanography, 17: 13.1-13.13.
Channell, J.E.T., Galeotti, S., Martin, E.E., Billups, K., Scher, H.
& Stoner, J.S. 2003. Eocene to Miocene magnetostratigraphy,
biostratigraphy, and chemostratigraphy at ODP Site 1090
(sub-Antarctic South Atlantic). Geological Society of America Bulletin, 115: 607-623.
Gibbs, S.J., Bralower, T.J., Bown, P.R., Zachos, J.C. & Bybell,
L.M. 2006. Shelf and open-ocean calcareous phytoplankton
assemblages across the Paleocene-Eocene Thermal Maximum: Implications for global productivity gradients. Geology, 34: 233–236. doi: 10.1130/G22381.1.
Kennett, J.P. & Stott, L.D. 1990. Proteus and proto-Oceanus: ancestral Paleogene oceans as revealed from Antarctic stable
isotopic results; ODP Leg 113. In: P.F. Barker, J.P. Kennett etal. (Eds). Proceedings ODP, Scientific Results, 113: 865– 880.
Lear, C.H., Elderfield, H. & Wilson, P.A. 2000. Cenozoic deepsea temperatures and global ice volume from Mg/Ca in benthic foraminiferal calcite. Science, 287: 269–272.
Miller, K.G., Wright, J.D. & Fairbanks, R.G. 1991. Unlocking theice house: Oligocene-Miocene oxygen isotopes, eustasy, andmargin erosion. Journal of Geophysical Research, 96: 6829–
6848.
Persico, D. & Villa, G. 2004. Eocene-Oligocene calcareous nan-

92

Abstracts

nofossils from Maud Rise and Kerguelen Plateau (Antarctica): Palaeoecological and palaeoceanographic implications.
Marine Micropaleontology, doi: 10.1016/j.marmicro.
2004.05.002.
Villa, G., Fioroni, C., Pea, L., Bohaty, S. & Persico, D. Submitted. Middle Eocene-Late Oligocene climate variability:
calcareous nannofossil response at Kerguelen Plateau, Site
748. Marine Micropaleontology.
Villa, G. & Persico, D. 2006. Late Oligocene climatic changes:
Evidence from calcareous nannofossils at Kerguelen Plateau
Site 748 (Southern Ocean). Palaeoceanography,
Palaeoclimatology, Palaeoecology, 231: 110-119.
Zachos, J.C., Pagani, M., Sloan, L., Thomas, E. & Billups, K.
2001. Trends, rhythms, and aberrations in global climate 65
Ma to Present. Science, 292: 686–693.
Zachos, J.C., Quinn, T.M. & Salamy, K.A. 1996. High-resolution(104 years) deep-sea foraminiferal stable isotope records ofthe Eocene – Oligocene climate transition. Paleoceanography, 11: 251–266.

Abstracts

Calcareous nannofossils as paleoproductivity indicators in
sediments from the southeastern Sulu Sea
Alyssa M. Peleo-Alampay, Deborah N. Tangunan
This study investigates calcareous nannofossils from two
sediment cores collected from the Sulu Sea in the southwestern Philippines during Philex cruise Leg 2 onboard
R/V Melville in December 2007. These two core sites fromthe southeastern Sulu Sea sub-basin were chosen for theirdifference in productivity, based on present-day chlorophyll data. The high productivity site, Core MC10, is located closer to the coast of Zamboanga Peninsula at
8˚23.10’N, 122˚09.15’E and 4022m water depth, while
Core MC8 is located in the central portion of the sub-basin
at 8˚38.97’N, 121˚31.83’E and 4492m water depth.
Sulu Sea is a marginal, enclosed oceanic basin that is
unique in its warm and oxygen-deficient bottom waters. It
exchanges waters with the South China Sea, Sulawesi Sea
via the Sibutu Strait, and with the Pacific through the Bohol
Sea. Today, it is one of the most productive fishery areas of
the Philippines that is increasingly exposed to anthropogenic activities. High chlorophyll-a maxima have been
observed during the northeast monsoon in recent times in
Sulu Sea waters off the coast of Zamboanga. Studying thesediment core in this area is a good opportunity to trace theupwelling history through time and compare it with theother study site.
Previous nannofossil studies show that some species
can be used as paleoproductivity indicators. This researchutilizes the lower photic-zone dweller, Florisphaera profunda as a proxy for non-upwelling or low-productivity
events. Higher abundances of upper photic zone species,
such as Gephyrocapsa oceanica, common in marginal sea
sediments, are used as upwelling or higher-productivity indicators.

93

94

Abstracts

Nannofossil and environmental changes across the
Sinemurian/Pliensbachian boundary in the Lusitanian Basin(S. Pedro de Moel, Portugal)
Julien Plancq, Stefano Palmerini, Vincent Grossi, Emanuela Mattioli, Bernard
Pittet, George Yordanof, François Fourel, Luis Vitor Duarte, François Baudin
The Sinemurian/Pliensbachian boundary is characterized
by an important event in the history of coccolith diversification, namely the first occurrence of Similiscutum (placolith coccoliths). However, nannofossil assemblages fromthis time interval are still poorly studied. In this work, anintegrated study of calcareous nannofossils (absolute andrelative abundance), inorganic (carbon and oxygen isotopes) and organic geochemistry (biomarkers) is presented.
Nannofossil preservation is moderate to good in the studied samples. Delicate structures, such as the long spine of
Parhabdolithus liasicus liasicus, are commonly preserved.
Some bio-events are reported from San Pedro de Moel. The
first occurrences of Mitrolithus lenticularis and Crepidolithus crassus are recorded in the Late Sinemurian, respectively ~20 and ~15 m below the Sinemurian/
Pliensbachian boundary, as defined by ammonites. The firstoccurrence of Similiscutum is observed ~3 meters above
the Sinemurian/Pliensbachian boundary. Few specimens of
Mazaganella are recorded from the base of the section.
Sedimentological data indicate a sea-level drop close
to the Sinemurian/Pliensbachian boundary at the studied
site. Nannofossil abundances per gram of rock are the lowest during the sea-level low, probably because of the reduction of the ecospace for the development of awell-diversified nannoplankton community. Although
Schizosphaerella spp. (a probable calcareous dinoflagellate) is always dominant in the analysed samples, coccolith proportion progressively increases in the basal
Pliensbachian. The percentage of Parhabdolithus liasicus
liasicus and P. liasicus distinctus that are very common in
the assemblage seem to be inversely correlated. Averagerelative abundance of Mitrolithus jansae is 10% in theUpper Sinemurian samples, but increases up to 30% in theLower Pliensbachian. Our results are similar to those presented for the same section by N. Perilli in Duarte et al.
(2006), although this work only deals with qualitative nannofossil data.
Environmental conditions favorable to organic matter(OM) accumulation occurred in the Late Sinemurian (Raricostatum Zone), but OM-poor sediments are recorded in
the Early Pliensbachian. The changes observed in the nannofossil assemblage composition may be the response of
the nannoplankton community to environmental changes
occurring across the Sinemurian/Pliensbachian. However,
because of the scarcity of works dealing with ecologicalpreferences of Lower Jurassic nannofossil taxa, we are atpresent unable to interpret them. The comparison of nannofossil assemblage composition and data derived from inorganic and organic geochemistry should enable us tobetter understand the ecology of some of the most ancient
coccolithophorids.
Reference
Duarte, L.V., Perilli, N., Antonioli, L., Rodrigues, R., Cabral,
M.C., Dino, R. & Azerêdo, M.C. 2006. Evidências sedimentologicas, geoquimicas (COT) e micropaleontologicas nas facies bituminosas do Sinemuriano termianl de Agua deMadeiros (Portugal). VII Congresso Nacional de geologia,
2006, Universidade de Evora: 633-636.

Abstracts

95

Productivity response to the SST and hydrography change
in the Tagus prodelta during the Younger Dryas and theHolocene
Channarayapattana Prabhu, Teresa Rodrigues, Jose-Abel Flores, Antje Voelker,
Fatima Abrantes
A sediment core recovered from the Tagus prodelta (90 mwater depth) in the Portuguese Margin has been analysed
for the coccolithophore assemblage, planktonic and benthic foraminifera oxygen isotopes and the biomarkers, forreconstructing the primary productivity variations during
the Holocene. The chronology, based on 10 AMS 14C dates,suggests that the sediment sequence extends up to the last
13.5 cal yr BP.
The alkenone-based SST, and the δ18O of G. bulloides,
suggest cooler surface water (~8˚C) conditions during theYounger Dryas (YD). This period was also characterised
by low primary productivity as indicated by the G.
muellerae abundance and low coccolithophore accumulation rates. However, the δ18O of benthic foraminifera
species A. beccari shows that the bottom water conditions
were different from surface conditions.
Termination 1B is associated with 1 ‰ G. bulloides
δ18O and 10˚C SST shifts. The primary productivity increases with rising temperature. The dominance of the coccolithophore species Gephyrocapsa oceanica and small
Gephyrocapsa is recorded for this period and also the
Holocene. The Holocene, particularly the last 8 cal kyr BP,
witnesses a decrease in SST from 19˚C to 15˚C. A gradualincrease in coccolithophore accumulation rate indicates
that, in spite of decreasing SST, primary productivity increased. The fresh water influx from the Tagus River could
have changed the surface water hydrography and triggered
higher primary production because the river water discharges important amounts of nutrients to the prodelta.
The sudden shift in δ18O of G. bulloides around 10, 8.2
and 5.6 cal kyr BP, could correspond to the abrupt cooling
events recorded in different parts of the Atlantic Ocean.
This suggests that the study area is influenced not only by
the river estuarine condition but also by the Atlantic Ocean
circulation.

96

Abstracts

Lower Jurassic (Domerian) calcareous nannoplankton
biogeography in the western Mediterranean area
Letizia Reggiani, Emanuela Mattioli
Quantitative studies have been carried out on Lower Jurassic calcareous nannofossils in order to assess a biogeographical distribution pattern within the western
Mediterranean area. Four sections have been studied in different paleogeographic settings, namely Peniche in the
Lusitanian Basin, Marcoux in the French Subalpine Basin,
Burano in the Umbria-Marche Basin, and Trionto in the
Ligurian-Piedmont Basin.
A total of 118 samples were analyzed for absolute andrelative abundance, Shannon diversity index, and
wt%CaCO3. Correlations between the sections have been
done by means of well-established nannofossil and ammonite integrated biostratigraphy. A careful checking ofpreservation state has been performed in each analyzed
sample.
In the Lower Jurassic, calcareous nannoplankton
species are commonly considered to be cosmopolitan.
However, significant changes in relative abundance ofspecies can be observed in different localities. Our study
indicates that Schizosphaerella spp. (a probable calcareous
dynocyst) dominates the assemblages in all studied sections, with percentage attaining 85%. This taxon is eurytopic but its relative abundance is systematically higher in
the Umbria-Marche Basin (Burano and Trionto sections)than in the Lusitanian and Vocontian Basins. Within the
coccoliths, the taxa showing the most significant biogeographic differences are: Crepidolithus crassus andMitrolithus jansae. Crepidolithus crassus exhibits higher
relative abundances within the Lusitanian and Vocontian
basins testifying to an affinity for the NW European settings. Conversely, Mitrolithus jansae dominates the assemblages in the Burano and Trionto sections, and istherefore associated with the Mediterranean domain.
Lower Jurassic palaeogeographic reconstructions indicate the existence of seaway connections between the NW
European and Mediterranean domains. Therefore, differences in relative and absolute abundances of specific taxa
within the studied area suggest a control of environmental
conditions on nannoplankton distribution. Several parameters may control nannoplankton distribution in the watercolumn. However, the most important parameter in thestudied localities seems to be related to nutrient supply inthe different paleogeographic settings.
The Mediterranean domain was characterized by perioceanic carbonate platforms, without surrounding emergedlands. This region was therefore characterized by generally
oligotrophic conditions in the considered time interval.
Conversely, the NW European domain was represented byshelves and shallow epi-continental basins, where more orless constant nutrient supplies were provided by surrounding emerged lands.

Abstracts

97

Spatial distribution of Pliensbachian (Lower Jurassic)
calcareous nannofossils within the Lusitanian Basin(Portugal)
Letizia Reggiani, Emanuela Mattioli, Bernard Pittet
Quantitative analysis of Pliensbachian calcareous nannofossils have been carried out on a proximal-distal transect
in the Lusitanian Basin (Portugal). The studied sections,
Tomar and Peniche, respectively represent the proximal
and the distal environments with respect to the emerged
land of the Iberian Meseta (to the east). The upper portionof the Vale das Fontes Fm (P. davoei and A. margaritatusammonite Zones) was studied in both sections and correlated by means of well-established ammonite and nannofossil integrated biostratigraphy. A careful analysis of thepreservation state of nannofossils was performed in thestudied samples. Preservation state is moderate to good in
the two settings, changes in nannofossil assemblages are
therefore considered as primary.
A total of 51 samples was analyzed for nannofossil absolute and relative abundances, wt%CaCO3 and species diversity. The analysis of calcareous nannofossil quantities(absolute abundance, percentage, average-abundance)shows changes in the community structure in the space(i.e., from proximal to distal), and vertically within thewater column. This record suggests a partitioning of habitats within the photic zone, and with respect to emergedlands. Proximal environments within the Lusitanian Basin
were probably more eutrophic, because of the presence of
emerged lands to the east (Iberian Meseta). This was thesource area for nutrients delivered into the basin. Distal environments were likely characterized by a relatively deeper
photic zone.
The assemblages recorded in the proximal setting exhibit
high mean relative abundance of placolith-bearing coccol-

iths (Lotharingius spp., Biscutum spp. and Similiscutumspp.) and of Schizosphaerella spp., while distal assemblages are dominated by Crepidolithus crassus andSchizospharella spp. C. crassus is interpreted as a deepdweller coccolithophorid, inhabiting preferentially distaland deeper settings in the Lusitanian Basin. Placolith-bearing coccoliths were more abundant under elevated trophic
conditions, and were more common in proximal settings,
with respect to emerged lands. The probable calcareous
dinocyst Schizosphaerella spp. proliferated in surface waters of both proximal and distal environments.

98

Abstracts

Calcareous nannofossils in petroleum exploration:
improving correlations using palaeoecological events
Frédéric Ricciardi
Calcareous nannofossils in petroleum research are powerful tools for high-resolution chronostratigraphy and calibration of seismic horizons. Nevertheless, standard studies
mainly focus on the chronostratigraphic aspect and only little attention is paid to potentially correlatable paleoecological and/or paleoclimatic nanno-events. For example,
the relatively long-lasting Miocene nannozone NN4(2.5Myr; 15.7Ma to 18.2Ma) is only characterized by the
LAD (Last Occurrence Datum) of H. ampliaperta and theFAD (First Occurrence Datum) of S. heteromorphus. Using
the modified classification of Wei & Wise (1990) on
datasets of 3 offshore Angola wells, the CTW variations(Cool to Temperate/Warm species) suggest four synchronous warm events in agreement with the foraminiferal
planktic blooms usually recognized in the area. A first eventis recorded at the NN2/NN3 transition while NN4 can be
subdivided into three intervals using two intra-NN4 events.
A last correlatable warm event characterizes the NN4/NN5transition. The paleoenvironmental characterization of nannoflora can hence be used, at least regionally, as a powerful tool that may refine the standard chronostratigraphic
zonation.

Reference
Wei, W. & Wise, S.W. 1990. Biogeographic gradients of middle
Eocene-Oligocene calcareous nannoplankton in the South
Atlantic Ocean. Palaeogeography, Palaeoclimatology,
Palaeoecology, 79: 29-61.

Abstracts

Multi-species coccolithophore response to ananthropogenically-modified ocean
R.E.M. Rickaby, P.R. Halloran, I.R. Hall, E. Colmenero-Hidalgo, J. Henderiks
Coccolithophores are one of the most important pelagic
calcifying organisms in the present ocean to contribute tothe organic carbon and carbonate pump of pCO2 from theatmosphere into the deep ocean. As a major primary producer in the ocean, coccolithophores are responsible forfixation and drawdown of dissolved inorganic carbon into
the deep ocean via the biological pump. Coccolithophores
also calcify, and the production and export of calcium carbonate releases CO2. The net influence of coccolithophores
on pCO2 depends partly on the particulate inorganic:organic carbon ratio (PIC/POC).
Major questions surround the species-specific nature ofcoccolithophore calcification in response to rising atmospheric CO2 levels and the likely biogeochemical feedback
on future climate. Here we investigate the assemblage wide coccolithophore response to anthropogenically elevated pCO2 using both culture experiments and field
evidence from a North Atlantic core. The particle volume
distribution data from the coccolith size-fraction of a rapidly accumulating North Atlantic sediment core appear toindicate that coccoliths produced by the larger coccolithophore species present at this location increase in massin parallel with anthropogenic CO2 release, in contrast to
those of the smaller size, which decrease in mass. This contrasting behaviour is consistent with the results of our culture experiments of different species under conditions ofcarbonate chemistry which is decoupled from pCO2. A divergence between the calcification response of these two
coccolithophore size-groups could reflect contrasting physiological controls and evolutionary adaptation to pCO2.
This has significant implications for the realistic representation of an assemblage-wide CO2-calcification response
in numerical models.

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Paleocene calcareous nannofossil analysis of the Qreiya
section (Egypt) and the Eastern Venezuelan Basin
Olga M. Rodríguez V., Marie-Pierre Aubry
The present study focuses on the comparison of the zonal
schemes based on calcareous nannofossils from two
differents localities: the Qreiya section (Egypt) and theEastern Venezuelan Basin. In the first locality, calcareous
nannofossil assemblages were analyzed in order toestablish the geochronological frame of a 20m-thickinterval of the Dahkla Formation, which is exposed in the
Qreiya section. This section lies at the southern end ofGebel Abu Had, ~50 km NE of Qena (N Egypt). Seventy
samples were qualitatively and quantitatively analyzed insmear slides. Preservation is good and coccoliths areabundant. The section is comprised in the Zones NP4 (-412.3 m) and NP5 (12.6-16 m).
A biostratigraphic study was carried out in 10 wells in
the Eastern Venezuelan basin. All the samples were takenfrom the Vidoño Formation. Fifty samples were analized
in smear slides. The Vidoño Formation belongs to theZones NP5 to NP9, preservation is poor and coccoliths are
rare. According to Pindell et al. (1998), during the Early
Paleocene this area was exposed, forming part of theforebulge related to the Paleogene foreland basin. In the
Late Paleocene a marine sedimentation occurred again.
References
Pindell, J.L., Higgs, R. & Dewey, J.F. 1998. Cenozoic palinspastic
reconstruction, paleogeographic evolution, and hydrocarbon
setting of the northern margin of South America. In: J.L.
Pindell & C.L. Drake (Eds). Paleogeographic Evolution and
Non-glacial Eustacy of Northern South America, SEPM
Special Publication: 45-86.

Abstracts

Evolution of the coccolithophore assemblages during theLast Deglaciation in ODP Site 1233 (southeastern Pacific
Ocean)
Mariem Saavedra-Pellitero, José-Abel Flores, Francisco Javier Sierro
ODP Site 1233 is located 40 km offshore southern Chile(41˚0.01’S, 74˚26.99’W at 838 m water depth) in a small
fore-arc basin on the upper continental slope isolated fromturbidity currents. At this location, the mean sedimentation
rates were extremely high (ca. 100cm/kyr) during the
Holocene, and the records show a pronounced variability(in compositional changes, and in marine and oceanic paleoenvironments; Lamy et al., 2004) on multi-centennial
to millennial timescales (Mix et al., 2003). Given thesecharacteristics, this ODP site is very sensitive to even small
past oceanographic changes.
The lack of high resolution paleoceanographic records
from the South Pacific during the last glacial period andthe following deglaciation, led us to study the biologicalresponses to climatic events in this region over the last
70kyr using coccolithophores.
The coccolith record has been shown to be responsive
to millenial-scale oscillations and variations in the positionof current systems. Smear slides were prepared to assess
the relative abundance of coccolithophore taxa and coccolith fluxes using the Flores & Sierro technique (1997),
using a petrographic microscope (1000X). Additional studies were performed under scanning electron microscope,using a combined technique of filtration and dilution (Andruleit, 1996).
One of the objectives of this work was the study of theLast Deglaciation and Termination I. Given this objective,
the resolution was increased during the time interval from~24kyr to ~10kyr. High productivity was recorded during
the Last Glacial Maximum (23 to 19 kyr), while a marked
decrease occurred during the deglaciation, based on coccolith fluxes (NAR, Nannofossil Acumulation Rate). Variations in the coccolithophore assemblage point out cold andwarm consecutive episodes.
References
Andruleit, H. 1996. A filtration technique for quantitative studies
of coccoliths. Micropaleontology, 42: 403-406.
Flores J.-A. & Sierro, F.J. 1997. Revised technique for calculationof calcareous nannofossil accumulation rates. Micropaleontology, 4: 21-324.
Lamy, F., Kaiser, J., Ninnemann, U., Hebbeln, D., Arz, H.W. &Stoner, J. 2004. Antarctic timing of surface water changes off
Chile and Patagonian ice-sheet response. Science, 304: 19591964.
Mix, A.C., Tiedemann, R., Blum, P. & Shipboard Scientific Party
2003. Leg 202 Summary. Proceedings of the Ocean Drilling
Program, Initial Reports, 202: 145pp. College Station TX.

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A revised calcareous nannofossil biostratigraphic
framework for the Campanian-Maastrichtian interval
recovered by ODP Leg 207 on Demerara Rise, westernequatorial Atlantic
Anatoliy Shumnyk, Sherwood W. Wise, Jr.
Ocean Drilling Program (ODP) Leg 207 to Demerara Rise,a submarine plateau off Suriname, South America, recovered Cretaceous and Paleogene sediments to help elucidate
the paleoceanography of the equatorial Atlantic (Erbacher
et al., 2004; Mosher et al., 2007). In doing so, it recovereda Campanian-Maastrichtian sequence at all five of the sites
drilled (1257-1261) that records the opening of the Equatorial Atlantic Gateway that accompanied the final separation of South America from Africa and the continuous
deepening of the study area that followed.
Oxic conditions were well established by the late Campanian, when sedimentation on Demerara Rise changed
from hemipelagic to pelagic, and clayey chalk was being
deposited. In general, carbonate contents are initially about
35wt% and diagenetic calcite, carbonate debris, trace fossils, barite and pyrite crystals are abundant. Radiolarians
are well preserved, indicating high surface-water productivity, although planktonic foraminifers are absent or poorly
preserved. The lower Campanian-lower Maastrichtian zeolitic nannofossil claystone, however, gives way to Upper
Maastrichtian greenish gray nannofossil chalk with foraminfers and clay.
The Campanian-Maastrichtian nannofossil chalks,
clays and claystones show a reasonably diversified assemblage of calcareous nannofossils, although most holococcoliths are missing due to bathyal paleowater-depths.
Well-preserved nannofossils are abundant in the section,and their distribution patterns provide a number of biostratigraphic nannofossil events that allow revision of thecalcareous nannofossil zonation for equatorial regions suchas this. The major biostratigraphic events illustrated in Figure 1 consist of the following first and last occurrences(FOs and LOs): Micula prinsii, Lithraphidites quadratus,
Reinhardtites levis-Tranolithus orionatus, Uniplanarius trifidus, Broinsonia parca constricta, Eiffellithus eximius, andB. parca parca.
Equally important, however, secondary index species
have been delineated via quantitative and qualitative nannofossil data from Holes 1258A, 1259A and 1260A, andthese can be correlated throughout the study area. These
events (Fig. 1) are: acmes of Lithraphidites quadratus,
Bukryaster hayi and Lithastrinus quadricuspis; LO ofacmes of Kamptnerius magnificus, Gartnerago segmentatum, Ahmuellerella octoradiata and Zeugrhabdotus bicrescenticus; FO of acmes of Pseudomicula quadrata,
Prediscosphaera incohatus, Ahmuellerella regularis,
Lithraphidites praequadratus, Micula praemurus and K.
magnificus; LO of Quadrum gartneri and Zeugrhabdotus
diplogrammus; FO of Ceratolithoides amplector; and sig-

nificant increases in C. amplector and Staurolithites mielnicensis. The study has shown that no previously developed stratigraphic schemes can be strictly applied to thissequence. Instead, this example shows that a mix of quantitative and qualitative approaches provides broader opportunities for the application of Cretaceous calcareous
nannofossil biostratigraphies.
References
Erbacher, J., Mosher, D.C., Malone, M.J. et al. 2004. Proc. ODP,
Init. Repts., 207. College Station, TX (Ocean Drilling Program). doi:10.2973/odp.proc.ir.207.2004
Mosher, D.C., Erbacher, J. & Malone, M.J. (Eds). 2007. Proc.
ODP, Sci. Results, 207. College Station, TX (Ocean Drilling
Program). doi:10.2973/odp.proc.sr.207.2007

Abstracts

Figure 1: Campanian-Maastrichtian biostratigraphic framework for Demerara Rise based on ODP Leg 207 cores

103

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Variations in abundance and morphology of Watznaueria
britannica and W. barnesiae coccoliths in the Volgian
sediments of the Ivkino section, Russian Platform
Ekaterina Shcherbinina
Volgian black shales (Upper Jurassic) are documented inmany areas of the Russian Platform. The widely known
Gorodishche and Kashpir sections display many short hiatuses in this interval. The Ivkino section (Unzha River, left
tributary of Volga River, Kostroma Oblast) seems to be
more complete and shows sedimentary contrasts. Middle
Volgian deposits (6 m) are made up of a rhythmical alternation of black shale (BS) and claystone/marlstone layers.
Nannofossil assemblages of the Ivkino section significantly
differ from those of the Gorodishche and Kashpir sections,where boreal Stephanolithion atmetos and Crucibiscutum
salebrosum and high-fertility Biscutum constans and Zeugrhabdotus erectus are found (Kessels et al., 2003). In thesection studied, the two first species are absent; the otherspecies are common in underlying Kimmeridgian sediment(up to 28 and 12% respectively), but become almost absent
in Volgian deposits (<1%). Nannofossil assemblages aremainly composed of Watznaueria spp. (W. barnesiae/fossacincta, W. britannica/communis, W. ovata, W. manivitiae)
forming up to 70% of the total nannofossil assemblage inthe lower part of the sequence and up to 98% in its upper
part. The occurrence of this oligospecific assemblage,
showing moderate preservation, seems to be caused by primary effect rather than by diagenetic impact. Successive
occurrence of unique specimens of Conusphaera mexicana, Polycostella beckmannii and Helenea chiastia approximately mark the NJ20A-B and NJKA zones.
W. britannica quantities strongly decrease at the baseof the Volgian sediments (from 40-50 to 15-20%), but its
abundance slightly increases in isolated BSs and toward
the top of the sequence, while W. barnesiae shows an inverse trend, reaching 85% of the total assemblage in thelower part of the sequence and decreasing in the BSs. To
define morphological variation in different Watznaueria
groups as a response to paleoecological changes during
BSs accumulation, biometric measurements, including
lengths and widths of coccoliths and of central opening,were made on 100 specimens of W. barnesiae and W. britannica groups, using digitally-captured images in light microscope. There are no significant changes in W. barnesiae
size and ellipticity from the Kimmeridgian toward the topof the Volgian sediments. This implies an extreme r-selection mode for this taxon. W. britannica displays a rather
narrow continuum of both coccolith length (Lc = 5.0-8.2μm) and proportion of coccolith and central opening
lengths (Lc/Lo = 2.8-5.5) in Kimmeridgian sediments. This
continuum is interrupted in Volgian sediments, where twodifferent W. britannica morphotypes occur. One of them isrepresented by small coccoliths (Lc = 3.5-5.0 μm) with narrow central openings (Lc/Lo = 5.0-7.7); the second mor-

photype is represented by large coccoliths (Lc = 6.0-9.8μm) with a large central opening (Lc/Lo = 2.2-4.1). Ellipticity of W. britannica does not change significantly from
Kimmeridgian to Volgian sediments. The lack of transitional forms between the two morphotypes likely indicates
their different life-strategies or the affinity for different
habitats, e.g. different depths in a stratified water column.
Relative increase in number of W. britannica group toward
the top of the BS sequence implies its high adaptive potential under increased fertilization during BS accumulation.
References
Kessels, K., Mutterlose, J. & Ruffell, A. 2003. Calcareous nannofossils from late Jurassic sediments of the Volga Basin(Russian Platform): evidence for productivity-controlled
black shale deposition. International Journal of Earth Sciences, 92(5): 743-757.

Abstracts

105

Late Maastrichtian short-term warming events in the Boreal
Realm: nannofossil evidence from Denmark
Emma Sheldon
The climate of the Late Cretaceous was probably one of
the warmest in the history of the Earth, and global sea levels were high, resulting in marine transgression over large
continental masses (Surlyk et al., 2003; Lykke-Andersen& Surlyk, 2004). However the Maastrichtian was characterised by a long-term global cooling and the Upper Cretaceous – Danian chalk succession of Denmark represents
part of one of the largest and longest-lived cool-water carbonate platform deposits in the stratigraphic record. Basedon foraminifera, nannofossils and oxygen isotope data fromlow-latitude and southern high-latitude sites (e.g. Huber &Watkins, 1992; Li & Keller, 1998; Thibault & Gardin,
2006, 2007), it is inferred that the overall cooling in the
Maastrichtian was superimposed by two short-term intervals of increased temperature, followed by a global cooling
just prior to the K/T event.
Sparse published material exists concerning Maastrichtian nannofossil palaeoecology of the Boreal Realm.
However, a temperature increase in the Late Maastrichtianis inferred based on warm-water planktonic foraminifera
incursions reported from the North Sea Basin and theFaeroe-Shetland Basin (e.g. King et al., 1989; Bergen &Sikora, 1999; Akker et al., 2000) and from Northern
Jutland and Stevns Klint in Denmark (Troelsen, 1955; Hart
et al., 2005).
Due to extensive hydrocarbon exploration in the chalksof the North Sea, a plethora of routine nannofossil and microfossil biostratigraphy has been carried out on the Upper
Maastrichtian reservoir sections, but the nature of the hydrocarbon industry dictates that most data is highly confidential and remains unpublished. This study presents
nannofossil data from the Boreal Realm which ties in with
global studies on the Late Maastrichtian palaeoclimaticfluctuations. A high-resolution quantitative nannofossil
study of 8 Upper Maastrichtian chalk cores from the Danish Central Graben and Danish Basin reveal small but significant shifts in taxa thought to have been sensitive totemperature fluctuations (Watznaueria barnesiae, Kamptnerius magnificus, Nephrolithus frequens). Two short-termwarming events are inferred in the Late Maastrichtian, one
in UC20bBP and one in UC20dBP, followed by a terminal
Cretaceous cooling.
References
van den Akker, T.J.H.A., Kaminski, M.A., Gradstein, F.M. &Wood, J. 2000. Campanian to Palaeocene biostratigraphy andpalaeoenvironments in the Foula Sub-basin, west of Shetland
Islands, UK. Journal of Micropalaeontology, 19: 23-43.
Bergen, J.A. & Sikora, P.J. 1998. Microfossil diachronism insouthern Norwegian North Sea chalks: Valhall and HodFields. In: R.W. Jones & M.D. Simmons (Eds). Biostratigraphy in Production and Development Geology. Geological Society, London, Special Publications, 152: 85–111.

Hart, M.B., Feist, S.E., Håkansson, E., Heinberg, C., Price, G.D.,
Leng, M.J. & Watkinson, P. 2005. The Cretaceous–Palaeogene boundary succession at Stevns Klint, Denmark:Foraminifers and stable isotope stratigraphy. Palaeogeography, Palaeoclimatology, Palaeoecology, 224: 6–26.
Huber, B.T. & Watkins, D.K. 1992. Biogeography of Campanian–Maastrichtian calcareous nannoplankton in the region of
the Southern Ocean: paleogeographic and paleoclimatic implications. In: The Antarctic paleoenvironment: a perspective
on global change. Antarctic Research Series, 56: 31–60.
King, C., Bailey, H.W., Burton, C.A. & King, A.D. 1989. Cretacceous of the North Sea. In: D.G. Jenkins & J.W. Murray(Eds). Stratigraphical Atlas of Fossil Foraminifera. Ellis Horwood Ltd, Chichester: 372-417.
Li, L. & Keller, G. 1998. Maastrichtian climate, productivity andfaunal turnovers in planktic foraminifera in South Atlantic
DSDP Sites 525A and 21. Marine Micropaleontology, 33: 55–
86.
Lykke-Andersen, H. & Surlyk, F. 2004. The Cretaceous–Palaeogene boundary at Stevns Klint, Denmark: inversion tectonics
or sea-floor topography? Journal of the Geological Society,London, 161: 343–352.
Surlyk, F., Dons, T., Clausen, C.K. & Higham, J. 2003. Upper
Cretaceous. In: D. Evans, C. Graham, A. Armour & P.
Bathurst (Eds). The Millennium Atlas: Petroleum Geology of
the Central and Northern North Sea. The Geological Societyof London: 213–233.
Thibault, N. & Gardin, S. 2006. Maastrichtian calcareous nannofossil biostratigraphy and palaeoceology in the Equatorial Atlantic (Demerera Rise, ODP Leg 207 Hole 1258A). Revue deMicropaléontologie, 49: 199-214.
Thibault, N. & Gardin, S. 2007. The Late Maastrichtian nannofossil record of climate change in the South Atlantic DSDP
Hole 525A. Marine Micropaleontology, 65: 163-184.
Troelsen, J.C. 1955. Globotruncana contusa in the White Chalkof Denmark. Micropaleontology, 1: 76–82.

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Campanian-Maastrichtian nannofossil biostratigraphy of the
Boreal Realm (Danish Basin chalks)
Emma Sheldon
Recently, two boreholes were drilled in the Danish Basin(Stevns-1 and Stevns-2), close to the well-known K/Tboundary section at Stevns Klint; the aims included sedimentology, isotopes, biostratigraphy and palaeoecology of
the chalks. The Danish Basin chalks comprise a system
sculpted by energetic, long-lasting contour currents into
ridge, drift, moat and valley systems (Lykke-Andersen &Surlyk, 2004; Surlyk & Lykke-Andersen, 2007). This presentation focuses on the Campanian to uppermost Maastrichtian biostratigraphy of the Stevns-1 well (Sheldon, inpress).
The succession consists broadly of Upper Campanian–lowermost Maastrichtian bioturbated chalk succeeded by
Lower Maastrichtian alternating chalks and marls. The
Upper Maastrichtian part comprises almost pure chalk withsome intervals of flint-rich chalk and marly horizons(Stemmerik et al., 2006).
The Stevns-1 well (with 100% core recovery) was
drilled on a Maastrichtian positive ridge structure within
the ridge, moat and valley complex. The Stevns-1 well is
the thickest completely cored section (456 m) through theUpper Campanian–Maastrichtian in northwestern Europe.
It therefore constitutes a significant biostratigraphic andpalaeoecological reference for this interval.
The core from the Stevns-1 well comprises ‘Campanian–Maastrichtian boundary interval’, Maastrichtian andDanian chalk. The ‘Campanian–Maastrichtian boundaryinterval’ is referred to subzones UC16dBP to UC16aBP and
the Maastrichtian (Tor Formation) spans UC20dBP to UC17
(after Burnett et al., 1998 and Network Stratigraphic Consultancy Ltd in Fritsen, 1999). The only apparent missing
section appears to be Zone UC18, probably explained by
the presence of minor firmgrounds, which were revealedby the lithological study.
A total of 64 species were encountered for the Maastrichtian and 71 for the ‘Campanian/Maastrichtian boundary interval’. Nannofossil preservation compares
favourably with that of North Sea chalks (Sheldon, 2006).
Previously unreported nannofossil events include the extinction of Helicolithus trabeculatus and increase in abundance of Prediscosphaera grandis in the Upper
Maastrichtian, and extinction of Zeugrhabdotus praesigmoides in the ‘Campanian/Maastrichtian boundary interval’. Additional nannofossil events, which appear tocontradict those of the established schemes, are discussed.
References
Burnett, J.A. with contributions from Gallagher, L.T. & Hampton, M.J. 1998. Upper Cretaceous. In: P.R. Bown (Ed.). Calcareous
Nannofossil
Biostratigraphy.
BritishMicropalaeontological Society Series. Chapman &Hall/Kluwer Academic: 132–199.

Fritsen, A. 1999. A Joint Chalk Stratigraphic Framework. Volume 1. Joint Chalk Research Program Topic V. NorwegianPetroleum Directorate: 206pp.
Lykke-Andersen, H. & Surlyk, F. 2004. The Cretaceous–Palaeogene boundary at Stevns Klint, Denmark: inversion tectonics
or sea-floor topography? Journal of the Geological Society,London, 161: 343–352.
Sheldon, E. 2006. Upper Maastrichtian-Danian nannofossils of
the Danish Central Graben and the Danish Basin: a
combined biostratigraphic-palaeoecological approach.
Unpubl. PhD thesis, Univ. College London, London: 354pp.
Sheldon, E. In press. Upper Campanian – Maastrichtian calcareous nannofossil biostratigraphy of the Stevns-1 borehole,Denmark. Journal of Nannoplankton Research.
Stemmerik, L., Surlyk, F., Klitten, K., Rasmussen, S.L. &Schovsbo, N. 2006. Shallow core drilling of the Upper Cretaceous Chalk at Stevns Klint, Denmark. Geological Surveyof Denmark and Greenland Bulletin, 10: 13-16.
Surlyk, F. & Lykke-Andersen, H. 2007. Contourite drifts, moats
and channels in the Upper Cretaceous chalk of the Danish
Basin. Sedimentology, 54: 405–422.

Abstracts

Nannolithofacies: an alternative method, using minerals
and calcareous nannofossils, for hydrocarbon reservoir
characterization and stratigraphic correlation
Seirin Shimabukuro, Armando Antônio Scarparo Cunha
Nannolithofacies is proposed as an alternative sediment
analysis method, combining two previously known, independent sediment analyses: calcareous nannofossils andheavy minerals. The method consists of the analysis andinterpretation of the calcareous nannofossil and mineralcontent of smear-slides by means of a petrographic microscope. The use of a high-resolution calcareous nannofossil
biostratigraphic framework, coupled with mineral analysis, allows us to distinguish different sandstone bodies andseal rocks in turbiditic systems. Our experience has shownthat authigenic minerals, such as anatase, dolomite andpyrite are suitable for this purpose. Other common allochthonous heavy minerals in sediments, such as zircon,
tourmaline, granade, biotite and rutile, are recognizable insmear-slides and they are considered good indicators tocharacterize the individual reservoir and its provenance.
Although qualitative, this method constitutes a useful toolin specific horizontal-well drilling operations (geo- andbiosteering). Provided that time and precision are criticalparameters in petroleum exploration, we stress that the nannolithofacies method, along with several independent studies, such as mineralostratigraphy, litho- and biostratigraphy
could be a valuable alternative, at low cost.

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Abstracts

The last 20kyr reconstruction of the western Mediterranean
Sea and north-western African margin from coccolithchemistry
Débora Simón-Baile, Patrizia Ziveri, Heather Stoll, José-Abel Flores, Francisco
Javier Sierro
The Alboran Sea is situated within a transition zone between the Mediterranean Sea and the Atlantic Ocean; thisexceptional location is particularly sensitive to record theconnections between both areas. It records and amplifies
the smallest climatic changes occurring at the mid-latitude
regions, however, there are few data about the primary
production pattern in the area and the influence of theAtlantic Ocean as the major source of nutrients.
The present work concerns the study of two high-resolution calipso piston cores obtained during Marion
Dufresne cruises. MD95-2043 was recovered from the Alboran Sea (WM) at 36˚N-2˚W and 1841m water depth, andMD03-2705 DUST was recovered from 3100 m water
depth at 18˚N-21˚W off Mauritania-Senegal (NWA).
Restricted coccolith fractions were analyzed for Sr/Ca
ratio and stable isotopes to reconstruct productivity and sea
surface temperature during the last 20kyr, and to assess theinteractions and latitudinal gradient between the western
Mediterranean Sea (WM) and the north-western African
margin (NWA).
Repeated decanting and microfiltering techniques allow
separation and concentration of sediment fractions dominated to high degrees by the coccolith-carbonate from asingle species. The cosmopolitan Emiliania huxleyi and thesurface dwellers Helicosphaera carteri and Calcidiscus
leptoporus were isolated from every sample, even when
their abundances in the original sample were low.
Different fractions from the same sample showed anoffset in the isotopic ratios that is in agreement with the
non-equilibrium effects obtained from previous culture experiments. The Mediterranean core shows a wider range ofisotopic values related to a greater sensibility of the area toclimatic and oceanographic variations.

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109

Variations in surface-water conditions at the NW Iberianmargin during the last ~50kyr, as revealed by coccoliths
Katharina Stolz, Karl-Heinz Baumann, Till J.J. Hanebuth
We present results from a Late Glacial and Holocene sediment sequence from the Northeast Atlantic. The studied
gravity Core GeoB 11035-1 spanning 505 cm sediment recovery was taken at the north-western Iberian Margin off
the Galician coast during the cruise P-342 in 2006. The site
is located at 42˚10’N/9˚39’W in a water depth of 2045 m.
The area is dominated by wind-driven upwelling during
summer, downwelling in winter and, furthermore, terrestrial sediment input by rivers (Schmidt et al., 2002). Therewith the thickness of the surface water is subject toseasonality and shows strong variations between the winter and summer seasons (Fiúza et al., 1998).
The investigations cover the study of coccolith assemblages, as well as the analysis of fine-fraction (<20 μm)
stable isotopes, assuming that the carbonate of the fine fraction is mainly build up by coccoliths.
In the lowermost 400 cm, probably spanning MIS 3 andMIS 2, the coccolith assemblage is dominated by the
species Emiliania huxleyi and Gephyrocapsa muellerae.
Coccolith numbers vary between c. 1000 and 3000 x106
coccoliths/g sediment. Few thermophilic species, such as
Syracosphaera or Helicosphaera, seem to prevail in phasesof the influence of warmer surface waters. This patternchanges with the onset of the Holocene, which is indicatedby a sharp increase in total coccolith numbers to more than
16 000 x106 coccoliths/g sediment pointing to an enhanced
productivity.
Fine-fraction δ18O values vary between 1.5 and -2.5
during the Last Glacial, showing a slight trend towards
lighter values. With the beginning of the Holocene, finefraction oxygen isotope values increase from -2.5 towards
heavier values around 1.5. Studies of Dudley et al. (1986)
have already shown that coccolith δ18O shows a positive
correlation of lighter values with increasing water temperatures, as it is also known and succesfully used in palaeoceanographic studies on planktic foraminifera. In ourstudies, we see, in contrast, an inverse trend to planktic
foraminifera oxygen isotope values from this area.
In near future, we will look for an explanation on thisproblem and extend our study on this site by using otherproxies for the reconstruction of surface water conditions.
References
Dudley, W.C., Blackwelder, P., Brand, L. & Duplessy, J.-C. 1986.
Stable isotopic composition of coccoliths. Marine Micropaleontology, 10: 1-8.
Fiúza, A.F.G., Hamann, M., Ambar, I., Díaz del Río, G.,
González, N. & Cabanas, J.M. 1998. Water masses and theircirculation off western Iberia during May 1993. Deep-Sea Research I: Oceanographic Research Papers, 45(7): 1127-1160.
Schmidt, S., van Weering, T.C.E., Reyss, J.-L. & van Beek, P.
2002. Seasonal deposition and reworking at the sedimentwater interface on the northwestern Iberian margin. Progressin Oceanography, 52: 331-348.

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Paleocene-Lower Eocene calcareous nannofossil
biostratigraphy of Bulgaria
Kristalina Stoykova
Outcrop samples from 50 sections spread all over the territory of Bulgaria, as well as core samples from five offshore wells (W Black Sea shelf) were analyzed forbiostratigraphy, using calcareous nannofossils. Martini’s(1971) work serves as a reference standard scheme for subdivision and correlation of thestudied sections.
A complete sequence of nine Paleocene and five
Lower
Eocenebiozonesisrecorded. Withineach biozone, asequence of successive bioeventsof first and/or last
occurrencesofstratigraphicallyreliable nannofossil taxa is observed. They are
utilized as additional markers inparticular parts ofthe zone.
This detailed
study has provided a total of 38
bioevents in the
Paleocene and 17
bioevents in the
Lower
Eocene(Figs 1A, B). The
selected bioevents
during the present
study are among
the most significant nannofossil
biohorizons, recently used to refine
Paleocene
andLower
Eocene calcareous
nannofossil biostratigraphic
framework(Agnini et al.,2007; Westerhold
et al., 2008). Their
recognition in thestudied sections allows the reliable correlation between the
Bulgarian sections and the sedimentary successions fromother parts of the world. The produced biostratigraphy isbased on the palaeontological identification of 212 species,
belonging to 62 calcareous nannofossil genera, besides theAbstracts

range of many species is refined.
References
Agnini, C., Fornaciari, E., Raffi, I., Rio, D., Röhl, U. &Westerhold, T. 2007. High-resolution nannofossil
biochronology of middle Paleocene to early Eocene at ODP
Site 1262: Implications for calcareous nannoplankton
evolution. Marine Micropaleontology, 64(3-4): 215-248.
Martini, E. 1971. Standard Tertiary and Quaternary calcareous
nannoplankton zonation. In: A. Farinacci (Ed.). Proc. II
Plankt. Conference. Roma, 1970. Tecnoscienza, 2: 739-785.
Westerhold, T., Röhl, U., Raffi, I., Forniaciari, E., Monechi, S.,
Reale, Bowles, V.J. & Evans, H. 2008. Astronomical
calibration of the Paleocene time. Palaeogeography,

111
Palaeoclimatology, Palaeoecology, 257(4): 377-403.

112

Abstracts

Paleocene hyperthermal events evidenced by calcareous
nannofossils in Bulgarian sections
Kristalina Stoykova, Marin Ivanov
We have carried out a detailed, purposeful study of calcareous nannofossil assemblages of many Paleocene sections, located in northern Bulgaria. During this study, we
have chanced upon some trustworthy evidences about therecord of two Paleocene hyperthermal events – the midPaleocene biotic event (MPBE) and the Paleocene-Eocene
thermal maximum (PETM).
MPBE. Until 2007, the MPBE was documented in theoceanic sections Shatsky Rise and Walvis Ridge only
(Bralower et al., 2003; Zachos et al., 2004). The first landbased locality has been recently described by Bernaola etal. (2007) at Zumaia section (W Pyrenees). According to
the last authors, the MPBE is positioned within the nannofossil zone NP6, at 4.5 m above the first occurrence of Heliolithus kleinpellii and 2 m below the C26r-C26nboundary. The nannoplankton response to this short-lived
warming event suggests a shift from cooler mesotrophic towarmer oligotrophic conditions, as evidenced by relative
abundance of selected calcareous nannofossil taxa
(Bernaola et al., 2007).
We report here the presence of particular clay-rich interval in two Bulgarian sections, at Kladorub (NW Bulgaria) and Byala (NE Bulgaria), characterized bysignificant calcareous nannofossil changes. At Kladorub
section, the distinct reddish clay layer (7-10 cm thick) occurred. It is situated within the upper part of NP 6 zone,
above the first occurrence of Discoaster bramlettei, and is
supposed to represent the sedimentary response of theMPBE. Calcareous nannofossil assemblage in the reddish
layer is characterized by the abundance of Heliolithus
kleinpellii, Coccolithus pelagicus and Toweius eminens. At
Byala section, the clay interval is grayish, dominated by
Heliolithus kleinpellii, H. cantabriae, Toweius tovae andEricsonia subpertusa. Further isotope (δ13C) and paleomagnetic studies are needed to perform in mid-Paleocene
sequences of both sections, in order to prove undoubtedly
the presence of MPBE.
PETM. First biostratigraphic evidences about the expression of the PETM in three Bulgarian sections,Kladorub, Riben and Bozhuritsa, have been recently produced (Stoykova & Ivanov, 2005; Stoykova et al., 2005).
Later on, it has been identified in the offshore section Yury
Shimanov, W Black sea shelf. The PETM is marked bysubstantial lithological turnover – sharp decrease of the carbonate content, as well as by major calcareous nannofossilchange across the Paleocene-Eocene boundary interval.
Samples have been collected usually at 0.5 m, but
within the PETM interval the sampling resolution has been
increased to 0.2 m. Calcareous nannofossils are common toabundant in all sections; only a few samples in the claydominated carbon dissolution interval contained rare, dissolution-resistant taxa or are barren of nannofossils.

Preservation varies from very good to moderate.
The interval investigated spans from the upper part of
NP9 zone to the lower part of NP10 zone. Calcareous
nannofossil assemblages show a major turnover across the
PETM interval. The P/E boundary coincides with theboundary between NP9/NP10 zones, which is placed at thefirst occurrence of Rhomboaster bramlettei. In all studiedsections, this boundary is drawn clearly above the onset ofthe event (Fig. 1).
The upper part of NP9 zone reveals an extremely diverse and abundant nannofloral assemblage, comprisingmore than 30 species. It is characterized by the species having their first occurrence here, such as Campylosphaera
eodela, Lophodolithus nascens and Transversopontis pulcher. The first occurrences of Discoaster mediosus, D. falcatus and D. limbatus are documented immediately below
the PETM in Bulgarian sections, along with the last occurrence of Scapholithus rhombiformis. Across the P/E boundary interval, a series of extinctions is recorded. The mostprominent is that of the genus Fasciculithus, which extinction is just below the onset of the PETM in NP9 zone.
Above the P/E boundary, i.e. in the Eocene part of
PETM interval, the nannofossil association is dominatedby Rhomboaster bramlettei (including R. cuspis), R.
spineus, Discoaster mediosus, D. falcatus, D. limbatus, D.
araneus, D. sp. aff. anartios. This association, called
Rhomboaster spp.-D. araneus (RD) association, was recently distinguished and proposed as reliable stratigraphic
proxy for the carbon isotope excursion at the PETM (Khan& Aubry, 2004).
The first occurrence of Discoaster diastypus is well
above the PETM interval, in the middle part of NP10 zone.
Neither Tribrachiatus digitalis, nor Rhomboaster contortus were recorded in our sections, which indicate the absence of the upper part of NP10 zone.
References
Bernaola, G., Baceta, J.I., Orue-Extebarria, X., Alegert, L.,
Martin-Rubio, M., Arostegui, J. & Dinares-Turell, J. 2007.
Evidence of an abrupt environmental disruption during themid-Paleocene biotic event (Zumaya section, western
Pyrenees). GSA Bulletin, 119(7-8): 785-795.
Bralower, T.J., Röhl, U., Petrizzo, M.R., Zachos, J., PremoliSilva, I., Thomas, D. 2003. Constraining the control on carbonate accumulation in deep sea sequences: a global
dissolution event in the early late Paleocene. GSA Abstracts,
35(6): 205.
Khan, A. & Aubry, M.-P. 2004. Provincialism associated with the
Paleocene/Eocene thermal maximum: temporal constraint.
Marine Micropaleontology, 52: 117-131.
Stoykova, K. & Ivanov, M. 2005. First data on the presence of
the Paleocene-Eocene Thermal Maximum in Bulgaria. C. R.
Acad. Bulg. Sci, 58(3): 297-302.

Abstracts

113

Stoykova, K., Ivanov, M., Dinares-Turell, J. & Spirovelli, M.
2005. Paleocene-Eocene Thermal Maximum – biostratigraphic and stable isotope data in Bulgarian sections. Bulg.
Geol. Soc., 80th Anniversary, Ann. Conf.: 21-23.
Zachos, J.C., Kroon, D. et al. 2004. Early Cenozoic extreme
climates: the Walvis Ridge transect. Proceedings ODP, Initial
Reports, 208 [online].

Figure 1: Correlation of the Bulgarian sections across the PETM interval: 1 – conglomerates; 2 – marls; 3 – clayey marls; 4 - rusty Fe-hydroxidesenriched marls; 5 – glauconitic marls; 6 – glauconites; 7 – glauconites with Ostrea shells (condensed level); 8 – marly limestones; 9 – dark-grey toblack clays; 10 – Fe-hydroxide concretions; 11 – cherty concretions; 12 – carbonate concretions; 13 – Ostrea shells and shell detritus; 14 – wash-out
surface114

Abstracts

Changes in size distribution of the Early Jurassic
nannofossil Schizosphaerella sp.: a new proxy for
paleoenvironmental reconstructions?
Guillaume Suan, Emanuela Mattioli, Bernard Pittet
Experimental studies suggest that increasing carbon dioxide concentrations due to anthropogenic emissions will
likely decrease the saturation state of the ocean with respect to calcium carbonate. This in turn should affect calcification of calcareous phytoplankton and could haveprofound and detrimental consequences for marine ecosystems (Orr et al., 2005). However, relationships between environmental conditions and phytoplankton calcification are
still unclear, and remain, furthermore, largely untested in
the geological record. Schizosphaerella incertae sedis, aprobable calcareous dinoflagellate, whose range is earliest
Jurassic to Late Jurassic, was one of the most important
carbonate pelagic producers during the Jurassic period andthus represents an ideal nannofossil taxon to address the
response of calcareous phytoplankton to past environmental changes.
Here we report size distribution measurements of
Schizosphaerella, calcium carbonate contents, and stable
isotopic compositions (δ18O and δ13C) of well-preserved
brachiopod shells from Lower Pliensbachian to Lower
Toarcian hemipelagic deposits of the reference section of
Peniche, Portugal. Nannofossil quantification indicates thatmost of the carbonate mud was not produced by nannofossils and was thus most likely imported from adjacent shallow-water platforms. The carbonate content and the size
variations of Schizosphaerella both show a close parallelism all along the studied interval, and largely co-vary
with the oxygen isotopic compositions of brachiopod
shells. Maximum mean diameters of Schizosphaerella arerecorded in the Late Pliensbachian, a period of cool climatic conditions, characterized by low carbon dioxide concentrations, while minimum sizes are recorded during the
Early Toarcian oceanic anoxic event, which is commonlyinterpreted as a time of elevated seawater temperatures andexceptionally high carbon dioxide concentrations (McElwain et al., 2005). Though it is tempting to attribute thesesize variations in terms of changes in carbon dioxide concentrations and calcium carbonate saturation, it is still unclear if carbon dioxide directly controlled the
biocalcification of this genus via carbonate saturation decrease, or indirectly via CO2-induced changes in environmental conditions (e.g., temperature, salinity, runoff andnutrient input).
References
McElwain, J.C., Wade-Murphy, J. & Hesselbo, S.P. 2005.
Changes in carbon dioxide during an anoxic event linked to
intrusion of Gondwana coals. Nature, 435: 479–482.
doi:10.1038/nature03618.
Orr, J.C. et al. 2005. Anthropogenic ocean acidification over thetwenty-first century and its impact on calcifying organisms.

Nature, 437: 681–686.

Abstracts

115

How did orbital cycles influence coccolith size fluctuations?
An example from the Early Pliensbachien (Early Jurassic) ofPeniche (Portugal)
Baptiste Suchéras-Marx, Emanuela Mattioli, Bernard Pittet, Gilles Escarguel,
Guillaume Suan
Though climate and environmental changes influence coccolithophorid (unicellular photoautotrophic algae) diversity, the relationships between fluctuation of size of
coccoliths (small calcite plates produced by coccolithophorids) and environmental parameters remain unclear.
In order to understand possible interactions between coccolith size variations and climate, a high-resolution (every
5 cm) biometric study of Crepidolithus crassus coccoliths
has been performed in the Early Pliensbachian (Early
Jurassic) hemipelagic deposits of Peniche (Portugal). Fourof the six measured parameters have cyclic patterns thatappear to be in phase opposition with calcium carbonate
contents of the sediments. Spectral analyses performed on
both size measurements and calcium carbonate contents
show that the size variations of C. crassus coccoliths are
related to Earth’s eccentricity and precession orbital cycles.
A closer analysis of morphologic disparity within the measured specimens through ‘mixture analysis’ reveals the existence of two distinct groups: a group called here ‘small
crassus’ with a mean size of ~6.5 μm, and a group called‘large crassus’ that averages a size of ~8.5 μm and dominates the assemblages during the studied interval.
C. crassus is generally interpreted as a deep-dweller(living in the lower photic zone) and its development could
have been greatly dependant on light supply. Accordingly,
the two morphotypes could have lived at different waterdepths due to differential buoyancy capacities. To test thishypothesis, a geometrical coccosphere reconstruction
model, based on coccolith biometry, was built and reveals
a linear relationship between coccolith size and coccosphere mass, thus confirming that smaller coccoliths may
have had overall higher buoyancies than larger ones. Consequently, it is suggested that changes in the water-column
transparency may have been an important controlling factor on replacement between the two groups, and hence theresulting coccolith mean size. This transparency may havebeen mainly controlled by both carbonate platform input
and storm recycled particulates in the photic zone, which
could thus explain the inverse relationship between calcium
carbonate contents and C. crassus size. Though, the ‘small
crassus’ group appears to be more abundant in organic matter-rich levels, suggesting a preference for nutrient-richwater bodies.

116

Abstracts

Diachroneic first occurrence of Marthasterites furcatus in
the Tethyan foreland basins (Outer Western Carpathians)
Lilian Švábenická
The depositional area of Tethyan foreland basins was
situated along the SE margin of the NW European
Platform, SE from its present location in the outer groupof nappes, Western Carpathians. This area was probably
connected with the epicontinental sea of the NW European
Plate, as it is the case for the Boreal-Tethyan transitional
path (Švábenická et al., 2002).
Here, the first occurrence (FO) of Marthasterites
furcatus was observed at two differrent stratigraphic levels(Figure 1):
1. Lower Turonian, zone UC6b, Silesian Unit. M. furcatusappears between FO Eprolithus moratus and FO Quadrum
gartneri.
2. Middle Turonian, zone UC9a, Waschberg Zone andŽdánice-Subsilesian Unit. Rare M. furcatus occurs
approximately at the same level as Lithastrinus
septenarius, after FO Eiffellithus eximius and before FO
Zeugrhabdotus biperforatus.

during the Cenomanian-Coniacian (Stráník et al., 1996).
The depositional area of the Silesian Unit was situated further northern (Golonka et al., 2006).
References
Golonka, J., Gahagan, L., Krobicki, M., Marko, F., Oszczypko, N.
& Slaczka, A. 2006. Plate Tectonic Evolution and Paleogeography of the Circum-Carpathian Region. In: J. Golonka& F. Picha (Eds). The Carpathians and their foreland. Geology and hydrocarbon resources. AAPG Memoir, 84: 11-46.
Stráník, Z., Bubík, M., Čech, S. & Švábenická, L. 1996. The
Upper Cretaceous in South Moravia. Věstník Českého
geologického ústavu, 71(1): 1-30.
Švábenická, L., Wagreich, M. & Egger, J. 2002. Upper Cretaceous
calcareous nannofossil assemblages at a transect from theNorthern Tethys to temperate realm in Central Europe. In: J.
Michalík (Ed.). Tethyan/Boreal Cretaceous Correlation.
Veda, Bratislava: 187-212.

The first occurrence of M. furcatus in the Middle Turonian was also observed in the epicontinental platform sediments of the Bohemian Cretaceous Basin. A seaway
between this area and the Ždánice-Subsilesian Unit existed

Figure 1: FO Marthasterites furcatus in the Outer Western Carpathians and Bohemian Cretaceous Basin. Data compiled by Stráník et al. (1996),
Švábenická et al. (2002) and this work. *rare, **common

Abstracts

117

Campanian-Maastrichtian nannofossil palaeoecology in the
Boreal Realm (Stevns-1 well, Danish Basin chalks)Nicolas Thibault, Niels Schovsbo, Emma Sheldon, Lars Stemmerik, Finn Surlyk
To date, very few studies have documented the distributionof Campanian–Maastrichtian boreal nannofossil assemblages (Friedrich et al., 2005; Sheldon, 2006). A comparison of these studies with our knowledge from the Tropical
Realm suggest that nannofossil species did not respond thesame way in both realms to climate change. For instance,in the Tropical Realm, cool-water taxa seem to highlightthe distinct climatic modes of the Maastrichtian (Thibault& Gardin, 2006, 2007), whereas no changes were noticed
in their distribution in the Boreal Realm, with respect toclimate change. This suggests that we need to better understand the palaeoecology of latest Cretaceous nannofossil taxa and especially that more data are needed from the
Boreal Realm.
Recently, two boreholes (Stevns-1 and Stevns-2) werecored close to the famous K/T boundary section at Stevns
Klint (Denmark), in order to investigate the sedimentology,
biostratigraphy and geochemistry of the Upper Campanian-Maastrichtian chalk succession (Stemmerik et al.,2006; Schovsbo et al., in press). Drilled on a palaeo–
seafloor high, the Stevns-1 well recovered 456 m of Upper
Campanian to basal Danian sediments with 100% recovery. The nannofossil biostratigraphy of this core has recently been investigated by Sheldon (in press, a). A nearlycomplete biozonation was documented from the Upper
Campanian to the K/T boundary, aside from the apparent
absence of zone UC18 (Sheldon, in press, a). To date,
Stevns-1 therefore represents the first continuous section
in northwest Europe through the uppermost Cretaceous andthe most expanded section worldwide. It is hoped that its
study will constitute a reference in the Boreal realm for extensive biostratigraphy, chemostratigraphy and palaeoceanography. The succession consists of Upper
Campanian–lowermost Maastrichtian bioturbated chalkwith rare, thin clay beds succeeded by interbedded lower
Maastrichtian chalk and marl. The Upper Maastrichtianpart comprises almost pure chalk with some intervals of
flint-rich chalk and few marly horizons (Stemmerik et al.,2006). The Stevns area has been buried to less than 600–
700 m during post-Danian time and the lack of extensiveburial diagenetic overprinting makes these sediments
highly suitable for geochemical and nannofossil palaeoecological analysis. The sites offer a unique opportunity to
document the evolution of boreal nannofossil assemblage
distribution with respect to climatic and environmental
changes.
This study will focus on the distribution of calcareous
nannofossil assemblages in Stevns-1 at two different timescales. At the sub-Milankovitch range, the distribution of
nannofossils in marl and chalk will be examined in order tohelp deciphering the distinct conditions leading to the deposition of these alternating cycles (primary vs. diagenetic

origin). At the million-year range, the evolution of the distribution of nannofossil assemblages are being comparedto that of stable isotopes in order to unravel the palaeoecological response of these fossil organisms to climatic modesin the latest Cretaceous Boreal Sea.
References
Schovsbo, N.H., Rasmussen, S.L., Sheldon, E. & Stemmerik, L.
In press. Correlation of carbon-isotope events in the Upper
Cretaceous chalk. Geological Survey of Denmark and Greenland Bulletin.
Sheldon, E. 2006. Upper Maastrichtian-Danian nannofossils of
the Danish Central Graben and the Danish Basin: a
combined biostratigraphic-palaeoecological approach.
Unpubl. PhD thesis, Univ. College London, London: 354pp.
Sheldon, E. In press, a. Upper Campanian-Maastrichtian calcareous nannofossil biostratigraphy of the Stevns-1 borehole,Denmark. Journal of Nannoplankton Research.
Sheldon, E. In press, b. Campanian-Maastrichtian nannofossil
biostratigraphy of the Boreal Realm (Danish Basin chalks).
12th International Nannoplankton Association Meeting, Lyon,
7–10 September, 2008, abstracts volume. Cambridge University Press, Cambridge.
Stemmerik, L., Surlyk, F., Klitten, K., Rasmussen, S.L. &Schovsbo, N. 2006. Shallow core drilling of the Upper Cretaceous chalk at Stevns Klint, Denmark. Geological Survey ofDenmark and Greenland Bulletin, 10: 13–16.
Thibault, N., & Gardin, S. 2006. Maastrichtian calcareous nannofossil biostratigraphy and palaeoecology in the Equatorial
Atlantic (Demerara Rise, ODP Leg 207 Hole 1258A). Revuede Micropaléontologie, 49: 199–214.
Thibault, N. & Gardin, S. 2007. The late Maastrichtian nannofossil record of climate change in the South Atlantic DSDP
Hole 525A. Marine Micropaleontology, 65: 163–184.

118

Abstracts

Calcareous nannofossil biostratigraphy (Upper Bajocian–Lower Bathonian) of the Ravin du Bès section (Bas Auran,
Subalpine Basin, SE France), evolutionary trends ofWatznaueria barnesiae and new enigmatic morphotypes of
the genus Rucinolithus
Daniele Tiraboschi, Elisabetta Erba
A biostratigraphic and evolutionary study based on calcareous nannofossils was performed on the Ravin du Bès
section (Bas Auran area, SE France), proposed as formal
candidate of Global Boundary Stratotype Section and Point(GSSP) for the base of the Bathonian stage (FernàndezLòpez et al., 2007). Semiquantitative estimates of total nannofloral abundance and single species abundance werecarried out. The following biohorizons were identified andcalibrated to ammonite biostratigraphy: the first occurrence(FO) of Watznaueria aff. W. barnesiae, the FO of Pseudoconus enigma; the FO of Rucinolithus sp.; the last occurrence (LO) of Hexalithus magharensis; the FO of
Stephanolithion speciosum octum and the FO of Watznaueria barnesiae. These results, consistent with biostratigraphic schemes previously proposed (Erba, 1988, 1990;
de Kaenel & Bergen, 1993; de Kaenel et al., 1996; Bown
& Cooper, 1998; Mattioli & Erba, 1999) confirm that calcareous nannofossils are good biostratigraphic markers for
the Bajocian/Bathonian boundary interval. Moreover, thefinding of P. enigma within the sub-Mediterranean
province allows a direct calibration between Tethyan and
Boreal nannofossil events and biozones.
This study showed an evolutionary trend from Watznaueria communis to Watznaueria barnesiae that seems to
support the theory of punctuated equilibrium rather than aphyletic gradualism.
We also documented the occurrence of new morphotypes of uncertain polycycloliths. These enigmatic nannoliths are very similar to specimens of the Cretaceous taxon
R. terebrodentarius, whose peculiar structure arises doubts
on its origin. In fact, as previously speculated (Tremola &Erba, 2002; Erba, 2004), R. terebrodentarius nannoliths
might be the result of CaCO3 precipitates or biocalcification by bacteria under peculiar oceanographic conditions,rather than products of coccolithophorid algae.
References
Bown, P.R. & Cooper, M.K.E. 1998. Jurassic. In: P.R. Bown
(Ed.). Calcareous Nannofossil Biostratigraphy. British Micropalaeont. Soc. Publ. Series. Kluwer Academic Publishers,
London: 34-85.
de Kaenel, E. & Bergen, J.A. 1993. New early and Middle Jurassic coccolith taxa and biostratigraphy from the eastern protoAtlantic (Morocco, Portugal and DSDP Site 547B). Eclogae
Geol. Helv., 86: 861-907.
de Kaenel, E., Bergen, J.A. & von Salis Perch Nielsen, K. 1996.
Jurassic calcareous nannofossil biostratigraphy of western Europe. Compilation of recent studies and calibration of bio-

events. Bull. Soc. Geol. Fr., 167: 15-28.
Erba, E. 1988. Calcareous nannofossils from the Bas Auran section. In: M. Innocenti, C. Mangold, G. Pavia & H. Torrens(Eds). A proposal for the formal ratification of the basal
boundary stratotype of the Bathonian stage based on a Bas
Auran section (S.E. France). 2nd International Symposiumon Jurassic Stratigraphy: 333-346.
Erba, E. 1990. Calcareous nannofossil biostratigraphy of some
Bajocian sections from Digne area (SE France). Mem. Descr.
Carta geol. Ital., 40: 237-356.
Erba, E. 2004. Calcareous nannofossils and Mesozoic Oceanic
Anoxic Events. Marine Micropaleontology, 52: 85-106.
Fernàndez-Lòpez, S.R., Pavia, G., Erba, E., Guiomar, M., Henriques, M.H., Lanza, R., Mangold, ?, Morton, N., Olivero, D.
& Tiraboschi, D. 2007. Formal proposal for the Global
Boundary Stratotype Section and Point (GSSP) of the Bathonian Stage, at the base of the Zigzag Zone in the Ravin du Bès
Section (Bas-Auran, Sudalpine Basin, SE France). International Subcommission of Jurassic Stratigraphy. Bathonian
Working Group Ballot: 1-43.
Mattioli, E. & Erba, E. 1999. Synthesis of calcareous nannofossil events in Tethyan Lower and Middle Jurassic successions.
Riv. Ital. Paleontol. Stratigr., 105: 373- 376.
Tremolada, F. & Erba, E. 2002. Morphometric analyses of Aptian
Assipetra infracretacea and Rucinolithus terebrodentarius
nannoliths: Implications for taxonomy, biostratigraphy andpaleoceanography. Marine Micropaleontology, 44: 77-92.

Abstracts

Quaternary calcareous nannofossil biostratigraphy andstable isotope stratigraphy (C and O) from middle slope,
northern portion of Campos Basin, Brazil
Felipe Antonio de Lima Toledo, Lucio Riogi Tokutake
This work presents paleoenvironmental interpretations forthe last 130 kyr in one middle slope core located in thenorthern portion of the Campos Basin. We used the methodof triangular co-ordinate diagram applied to calcareous
nannofossils. This method is used to estimate environmental characters by plotting nannofossil quantitative data
(Tokutake & Toledo, 2007; Toledo et al., 2005). It can be
useful for paleoceanographic and paleoproductivity studies. The same samples were collected for calcareous nannofossils and stable isotopes (C and O).
Calcareous nannofossil results show an absolute predominance of three taxa: Florisphaera profunda, Emiliania
huxleyi and Gephyrocapsa spp. Some estimates were madeby means of comparisons between the same species plottedin Okada’s triangle (Okada, 1992) in order to compare theeffect of temperature, depth and nutrient availability on
coccolithophore community.
Isotope stratigraphy reveals a good correlation with
δ18O isotopic stages. The carbon isotope stratigraphy datashows a good correlation with abundance variations ofGephyrocapsa spp., indicating variations in the nutrient
availability.
References
Okada, H. 1992. Biogeographic control of modern nannofossil
assemblages in surface sediments of Ise Bay, Mikawa Bay
and Kumano-Nada, off coast of central Japan. Memorie Di
Scienze Geologiche, 43: 431-449.
Tokutake, L.R. & Toledo, F.A.L. 2007. Bioestratigrafia denanofósseis calcários e Estratigrafia de Isótopos (C e O) do
Talude médio, Quaternário, porção N da Bacia de Campos,
Brasil. In: Ismar Carvalho, Rita Cassab, Cibele Schwanke,
Marcelo Carvalho, Antonio Fernandes, Maria Rodrigues,
Marise Carvalho, Mitsuru Arai & Maria Emília Oliveira(Eds). Paleontologia: Cenários da Vida, 2. Interciência Ltda.,
Rio de Janeiro: 395-410.
Toledo, F.A.L., Quadros, J.P., Santos, E.C. & Costa, K.B. 2005.
Análise paleoambiental em estudos quantitativos denanofósseis calcários: aplicação do diagrama triangular decoordenadas para o sudoeste do oceano atlântico. 10th
ABEQUA Congress, Gurapari, 1.

119

120

Abstracts

Seasonal control on Emiliania huxleyi coccolith calcificationin the Aegean Sea (E Mediterranean)
Maria V. Triantaphyllou, Margarita D. Dimiza, Eva Krasakopoulou, Elisa
Malinverno, Valia Avgoustidi, Valia Lianou
Morphometric analysis has been performed on Emiliania
huxleyi coccoliths from different locations of the Aegean
Sea (water and sediment trap samples). The modern
Aegean Sea is one of the most oligotrophic parts in theeastern Mediterranean Sea and a major area for deep water
formation (Zervakis et al., 2000; Lykousis et al., 2002).
A seasonal morphological variation has been observedin several E. huxleyi type A specimens, collected from discrete water samples in the Aegean Sea. The pattern revealed displays an increase in the size of coccoliths andcoccospheres, including a thicker inner tube-cycle (INT)of the distal shield, during winter and early spring months,
when the lowest SSTs (15-18˚C) are occurring and higher
HCO3- concentrations have been recorded.
The morphology of E. huxleyi shows considerable variation associated with size increase and, more specifically,
exhibiting overcalcified specimens.
Analogous highly-calcified specimens have beenrecorded during Holocene colder intervals, and have been
considered to represent a primary feature of the AegeanSea.
Our initial results hint at a possible link between higher
bicarbonate ion concentration, lower temperatures andstronger coccolithophore calcification in the field.
Since a number of other factors such as nutrients andlight intensity affect coccolithophore calcification, theabove evidence still remains to be further investigated.
References
Lykousis, V., Chronis, G., Tselepides, A., Price, N.B., Theocharis,
A., Siokou-Fragou, I., Wambeke, F. van, Danovaro, R.,
Stavrakakis, S., Duineveld, G., Georgopoulos, D., Ignatiades,
L., Souvermezoglou, A. & Voutsinou-Taliadouri, F. 2002.
Major outputs of the recent multidisciplinary biogeochemical researches undertaken in the Aegean Sea. J. Mar. Syst.,
33-34: 313-334.
Zervakis, V., Georgopoulos, D. & Drakopoulos, P.G. 2000. The
role of the North Aegean in triggering the recent Eastern
Mediterranean climatic changes. J. Geophys. Res., 105:
26103-26116.

Abstracts

121

Calcareous nannofossil evidence for Marine Isotopic Stage
31 (1Ma) in ANDRILL MIS Core (western Ross Sea,
Antarctica)
Giuliana Villa, Davide Persico, Sherwood S. Wise, Alessia Gadaleta
During the austral summer 2006, the ANDRILL Program
recovered a 1285-m-long succession of cyclic glaciomarine sediments from the McMurdo Ice Shelf (MIS). The
aim of the MIS Project was to obtain continuous Neogene(c.0-10Ma) glacial, glaciomarine, volcanic and biogenic
sediments that have accumulated in the region of the MIS(Ross Sea), nourished by ice flowing from the East Antarctic Ice Sheet (EAIS) outlet glaciers in the Transantarctic
Mountains.
The MIS AND-1B drill core represents the longest andmost complete (98% recovery) geological record from theAntarctic continental margin to date, and will provide a key
reference record of climate and ice-sheet variability
through the Late Neogene; detailed investigations of thisrecord will contribute for improving our knowledge ofAntarctica’s influence on global climate.
Preliminary on-ice analysis of the smear slides of the
Andrill core revealed calcareous microfossils (dinoflagellates, calciosponge spicula and small foraminifera) occurring with variable concentrations. The presence ofthoracosphaerid fragments in the smear slides of the first
600mbsf (Quaternary), probably belong to the species Thoracosphaera saxea (Stradner, 1961) and T. heimi (Kamptner, 1941) and other, potentially undescribed, species (Villa& Wise, 1998), suggesting either a peculiar adaptation tothis environment, due to their ability to develop cysts, or
warmer conditions at the time of their deposition, or a combination of both. However, they represent an additional element to use, along with the other proxies for inferring
palaeoenvironmental conditions of the core.
Subsequent shore-based analyses of 100 samples from86-96mbsf revealed for the first time the presence of Pleistocene coccolithophorids at these high southern latitudes(77˚S), including: Cocco. pelagicus, small Gephyrocapsa,
Retic. asanoi, Pseudoemil. lacunosa, Dictyo. productus,
Retic. sp., R. minutula, Thoraco. spp. Tertiary reworked
species include: Discoaster sp., Retic. hampdenensis, R.
pseudoumbilica, Dictyo. antarcticus, Cyclicargo. floridanus, Geminilith. rotula, Transverso. sigmoidalis and theUpper Cretaceous Rein. levis. As the lower temperature
limit for living calcareous nannoplankton is 2.5˚C, the presence of nannofossils from 86 to 96mbsf, though rare, is anindication of ice-free conditions and sea surface temperatures warmer than today in the Ross Sea. The presence ofnumerous volcaniclastic units and bio-siliceous sedimentsfrom 86.6 to 92.5mbsf indicate an extended period of openwater conditions, with no sea ice beyond the calving line.
An 40Ar/39Ar age of 1.015±0.004Myr on pumice at
85.20mbsf confirms the age assignment given by diatom
biostratigraphy (1.07Ma) for this interval. Accordingly, theshort normal magnetozone between 84.97 and 91.13mbsf iscorrelated with the Jaramillo Subchron (C1r.1n; Wilson etal., 2006).
The presence of nannofossils in the biogenic interglacial sediments is consistent with a warm episode of surface waters and open-marine conditions during the
Jaramillo Subchron, at ~1Ma, which corresponds with Marine Isotope Stage 31 (Naish et al., 2007). The ‘superinterglacial’ associated with Marine Isotope Stage 31 was thelast significant warm interglacial of the obliquity-dominated world, and may represent a precursor to the high-amplitude, eccentricity-dominated cycles that followed the
mid-Pleistocene climate shift. Climate proxies from otherstudies around Antarctica, like nannofossils and oxygenisotope stratigraphy at ODP Site 1165 (Villa et al., 2008),
and the presence of Thoracosphaera in a shelly carbonate
sequence at Cape Roberts 1 (Villa & Wise, 1998), also support the idea of a warming event during this time, suggesting that it was areally extended around the Antarctic
Continent, implying a total or partial collapse of the MIS.
The warm interval during the Jaramillo Subchron showsthat these areas were more climatically dynamic than previously thought and calls into question the notion that the
EAIS has remained in a stable polar condition since the late
Neogene. The warm surface water event reported here isespecially significant, given its proximal position to the
Antarctic ice sheet.
References
Kamptner, E. 1941. Die Coccolithineen der Südwestküste vonIstrien. Annalen des Naturhistorischen Museums in Wien, 51:
54–149.
Naish, T., Powell, R., Levy, R., Henrys, S., Krissek, L., Niessen,F., Pompilio, M., Scherer, R., Wilson, G. & the ANDRILMIS Science Team 2007. Synthesis of the Initial Scientific
Results of the MIS Project (AND-1B Core), Victoria Land
Basin, Antarctica. Terra Antarctica, 14(3): 317-327.
Stradner, H. 1961. Vorkommen von Nannofossilien im
Mesozoikum und Alttertiär. Erdöl-Zeitschrift, 77: 77–88.
Villa, G. & Wise, S.W. 1998. Quaternary calcareous nannofossils
from the Antarctic region. Terra Antarctica, 5(3): 479-484.
Villa, G., Fioroni, C., Pea, L., Bohaty, S. & Persico, D. Submitted. Middle Eocene-Late Oligocene climate variability: calcareous nannofossil response at Kerguelen Plateau, Site 748.
Marine Micropaleontology.
Wilson, G., Levy, R., Browne, G., Dunbar, N., Florindo, F., Henrys, S., Graham, I., McIntosh, W., McKay, R., Naish, T.,
Ohneiser, C., Powell, R., Ross, J., Sagnotti, L., Scherer, R.,
Sjunneskog, C., Strong, C.P., Taviani, M., Winter, D. & the
ANDRILL MIS-Science Team 2007. Preliminary Integrated
Chronostratigraphy of AND-1B Drill Core, ANDRILL McMurdo Ice Shelf Project, Antarctica. Terra Antarctica, 14(3):297-316.

122

Abstracts

Paleocene nannofossils from the Odessa Shelf(south-western Black Sea region)
Dennis Daniel Waga, Aida Sergeivna Andreeva-Grigorovich
In 2006 -2007, two boreholes (Odeska-6 and Odeska-20)
were drilled on the south-western part of the Ukrainian sector of the Black Sea. According to the geophysical welllog data, borehole Odeska-20 recovered sediments of the
Paleocene (1151-1621 m) and Eocene (692-1151 m).
We studied nannofossils from the Paleocene interval ofboth boreholes. The identified nannofossils had a moderate
to bad preservation. Four nannofossil zones of Martini(1971) and Okada & Bukry (1980) were identified: combined Cruciplacolithus tenuis-Chiasmolithus danicus zone
(NP2-NP3/CP1b-CP2), Fasciculithus tympaniformis(NP5/CP4), Heliolithus kleinpellii (NP6/CP5) and Heliolithus riedelii (NP8/CP7).
The combined C. tenuis-C. danicus zone (NP2NP3/CP1b-CP2) was distinguished only in borehole
Odeska-6 (int. 1544-1635 m). The most common species
are: Coccolithus pelagicus, Neochiastozygus sp., Toweius
sp., Thoracosphaera sp., Sphenolithus sp., Zygodiscus sp.,fragments of Braarudosphaera, Cruciplacolithus cf. C.
tenuis, Coccolithus sp., Chiasmolithus aff. C. danicus. Theinterval is also characterized by a large number of reworked
Cretaceous species: Watznaueria barnesiae, Arkhangelskiella cymbiformis, Micula staurophora, Broinsonia
parca, Kamptnerius? sp., Eiffellithus sp., Gartnerago sp.,etc. The lower two samples (3232, 3284) from the interval
1625.1-1625.2 m are assigned to the C. tenuis-C. danicus
zone, based on the presence of C. pelagicus and Neochiastozygus sp.
The F. tympaniformis (NP5/CP4) is present in bothboreholes: Odeska-6 (int. 1477.55-1548 m) and Odeska20 (int. 1544-1563.1 m). The typical species are: F. tympaniformis, F. cf. F. ulii, Ellipsolithus cf. E. macellus, Prinsius
sp., Braarudosphaera bigelowii, C. pelagicus, F. cf. F. involutus, Toweius sp., T. pertusus (craticulus), T. eminens,
Ericsonia subpertusa, F. pileatus?, Fascic. sp. The intervals are also characterized by the same reworked species asin the previous zone, but they are much rarer.
The H. kleinpellii (NP6/CP5) zone in Odeska-6(1475.55) and Odeska-20 (1513.22-1544 m) is identified
thanks to the FO of H. cf. H. kleinpellii. The nannofossil assemblage of the zone is characterized by Fascic. sp., F. cf.
F. ulii, F. cf. F. shaubii, Heliolithus sp., C. pelagicus,
Toweius sp., Thoracosphaera sp., Ericsonia robusta, Prinsius sp., Markalius inversus?, Chiasmolithus bidens, Coccolithus eopelagicus, Chiasmolithus consuetus. The upper
limit of the zone was not identified. It was set within thelower limit of the subsequent H. riedelii (NP8/CP7) zone.
H. riedelii (NP8/CP7) zone was established in bothboreholes Odeska-6 (int. 1424.21419.2 m) and Odeska-20(int. 1513.22-1457.95 m). Its lower limit was determinedthrough the FO of H. riedelii. In borehole Odeska-20, it isestablished within sample 5 (1457.95 m) where only four

species were identified: Thoracosphaera sp., Toweius sp.,C. pelagicus and reworked species W. barnesiae. Sample 5
was collected from a interval (1452.25-1469.25 m) that ispresented by non-carbonate grey sandstones and siltstones.
The identified zone is presented by an assemblage of T.
craticulus, Prinsius sp., C. pelagicus, Thoracosphaera sp.,
Heliolithus conicus, Sphenolithus cf. S. anarrhopus, Prinsius bisulcus, C. eopelagicus, H. kleinpellii, Discoaster cf.
D. elegans, Fascic. sp., F. tympaniformis, Heliolithus
cantabriae, Zygodiscus sigmoides, Pontosphaera sp., Ericsonia robusta, Chiasmolithus cf. C. consuetus, M. inversus, Fascic. cf. F. billii, Chiasmolithus danicus,
Sphenolithus primus, Discoaster sp. In the H. riedelii zone,
the number of reworked species decreases; they are represented by W. barnesiae, M. staurophora, Micula sp., Gartnerago sp., Eiffellithus sp., Cretarhabdus conicus?
According to the Stratigraphic Scheme of Southern
Ukraine (Makarenko et al., 1993) the combined C. tenuisC. danicus (NP2-NP3/CP1b-CP2) zone correlates with thelower part of the Bilokamian stage (Danian of the Geological Time Scale of Gradstein et al., 2004). The F. tympaniformis (NP5/CP4), H. kleinpellii (NP6/CP5) and H. riedelii(NP8/CP7) zones correlate with the Kachian (SelandianThanetian) stage.
Based on nannofossil research it is possible to suggestthat there are two unconformities. One is present within the
Bilokamian stage (borehole Odeska-6) and corresponds tothe zones E. macellus (NP4) and lower part of the F. tympaniformis (NP5/CP4) that are missing. The second one ispresent within the Kachian stage and corresponds to the absence of the Discoaster mohleri zone (NP7/CP6). With thehelp of the Geological Time Scale (Gradstein et al., 2004)
the relative duration for the first unconformity is estimatedto about 3.2 Myr; the second one lasted around 0.7 Myr.
References
Gradstein, F.M., Ogg, J.G. & Smith, A.G. 2004. The Paleogene
Period. A Geological Time Scale. Cambridge University
Press, Cambridge: 310-322.
Martini, E. 1971. Standard Tertiary and Quaternary calcareous
nannoplankton zonation. Proceedings II Plankton
Conference, Roma. Tecnoscienza, 2: 739-785.
Makarenko, D.E., Zelinskaya, V.A., Zernetskiy, B.F. et al. 1993.
Stratigraphic Scheme of Paleogene sediments of Ukraine forthe geological maps of the new generation. Graphic additions,
Kiev.
Okada, H. & Bukry, D. 1980. Supplementary modification andintroduction of code numbers to the low latitude coccolith
biostratigraphic zonation (Bukry, 1973; 1975). Marine
Micropaleontology, 5(3): 321-325.

Abstracts

123

Figure 1: SEM photographs of nannofossils from the Odeska Gas Field.
1. Heliolithus sp. (Borehole Odeska-20, 1489m); 2. Ericsonia sp. (Borehole Odeska-6, 1424.2m); 3. Toweius tovae (Borehole Odeska-6, 1424.2m); 4.
Prinsius bisulcus? (Odeska-6, 1424.2m); 5. Fasciculithus tympaniformis (Borehole Odeska-20, 1489m); 6. Neochiastozygus sp. (Borehole Odeska-6,,
1424.2m)

124

Abstracts

Calcareous nannofossil biostratigraphy of the Buchak andKiev Formations (Middle Eocene) of the central part of the
Ukrainian Shield
Dennis Daniel Waga, Aida Sergeivna Andreeva-Grigorovich
Paleogene sediments are widely distributed above the crystalline rocks of the Ukrainian Shield. The most complete
section of the Paleogene is located in the Southern Krivbass(Inguletsk quarry). The Middle Eocene is represented hereby the Voikovska, Rahmanivska, Malynivska, Staroinguletska and Borisfenska suites (Berezovskiy, 2000). The
first three correspond to the Buchak Formation of the
Lutetian stage; the Staroinguletska suite is equivalent with
the Kiev Formation of the Bartonian stage. The Borisfenska suite is assigned to the Lower Oligocene (Berezovskiy,2000). Despite a long period of paleontological researchwithin this area, the age of most of the suites remains
equivocal. Doubts mostly concern the age of the upper partof the Staroinguletska suite (Berezovskiy, 2000).
We studied nannofossils from sediments of the Malynivska (samples 1-9) and Staroingiletska (samples 10-19)
suites (Andreeva-Grigorovich et al., 2003; Waga, 2007).
Both formations are represented by terrigeneous (sandstone-clayey) and clayey (silty-mudstone) sediments andconstitute a total thickness of about 40m. Samples 1-4 fromthe lower half of the Malynivska suite did not contain any
nannofossils. Nannofossils appear in the upper part of thesuite (samples 5-7) where they are represented by an association of moderate- towell-preserved species: Coccolithus
pelagicus, Coccolithus eopelagicus, Ericsonia formosa,Ericsonia fenestrata, Reticulofenestra minuta, Discoaster
germanicus, Discoaster deflandrei, Discoaster barbadiensis, Discoaster elegans, Discoaster kuepperi, Nannotetrinasp., Nannotetrina fulgens, Chiasmolithus solitus, Rhabdosphaera sp., Transversopontis pulcheroides, Neococcolithus dubius, Discoaster binodosus binodosus, Discoasterdistinctus, Reticulofenestra dictyoda (Waga, 2007). Thesesamples were assigned to the Nannotetrina fulgens (NP15)
of Martini (1971) or Nannotetrina cristata (CP13) of
Okada & Bukry (1980) zonation.
The lower part of the Staroinguletska suite (samples 814) is characterized by similar species, but with the FO of
Rhabdosphaera truncata, Chiasmolithus consuetus,
Chiphragmalithus cristatus, Rhomboaster sp., Coronocyclus nitescens, Zygrhablithus bijugatus, Rhabdosphaera
creber (Waga, 2007). This section was correlated with theupper part of the Nannotetrina fulgens (NP15) zone ofMartini (1971).
Based on the FO of Discoaster bifax, the following interval (samples 15-19) was assigned to the Discoaster bifax(CP14a) Subzone of Okada & Bukry (1980). Apart fromthe zonal marker the most common species are: Transversopontis pulcheroides, Neococcolithus dubius, Reticulofenestra dictyoda, Discoaster tanii nodifer, Coccolithus
pelagicus, Reticulofenestra umbilica, Chiasmolithus gran-dis, Reticulofenestra hilliae.
In the paleoecological aspect, within the study area during the Middle Eocene existed a shallow to moderatelydeep paleobasin with warm to tropical conditions. Bothnannofossil zones contain species which, according to theclassification of Dmitrenko (1993), are typical for tropicalecological zone (Discoaster deflandrei, Sphenolithus moriformis, Cyclicargolithus formosus, Discoaster barbadiensis, Discoaster binodosus binodosus, Chiasmolithus
grandis, etc.). On the basis of the paleobionomical classification (Baldi-Beke, 1983), nannofossil assemblages arecharacteristic of an open-ocean (Coccolithus, Cyclicargolithus, Zygrhablithus, Discoaster tanii nodifer) to a shallow-water (Rhabdosphaera, Pontosphaera) environment(Waga, 2007).
These results allow us to conclude that the sedimentsof the Staroinguletska suite (Kiev Formation), which were
earlier believed to be equivalents of the Bartonian stage,
can be correlated indeed with both the Lutetian and theBartonian stages of the Geological Time Scale (2004).
References
Andreeva-Grigorovich, A.S., Berezovskiy, A.A. & Waga, D.D.O.
2003. Nannoplankton and Mollusks from the Eocene depositsof the Kryvoy Rog Iron Basin. Theoretical and practical aspects of the modern stratigraphy of the Phanerozoic of
Ukraine. Kiev: 3-5.
Baldi-Beke, M. 1984. The nannoplankton of the Transdanubian
Paleogene formations. Inst. Geol. Hungaricum., Pal., 43: 153222.
Berezovskiy, A.A. 2000. Local stratigraphic scheme of Paleogeneof the Kryvoy Rog Basin. Biostratigraphical and paleoecological aspects of event stratigraphy. Kiev: 43-45.
Dmitrenko, O.B. 1993. Biogeography of the Atlantic and Indian
Oceans in Cainozoic based on nannoplankton. Nedra,
Moscow: 175pp.
Gradstein, F.M., Ogg, J.G. & Smith, A.G. 2004. The Paleogene
Period. A Geological Time Scale. Cambridge University
Press, Cambridge: 310-322.
Martini, E. 1971. Standard Tertiary and Quaternary calcareous
nannoplankton zonation. Proceedings II Plankton Conference, Roma. Tecnoscienza, 2: 739-785.
Okada, H. & Bukry, D. 1980. Supplementary modification andintroduction of code numbers to the low latitude coccolith
biostratigraphic zonation (Bukry, 1973; 1975). Marine Micropaleontology, 5(3): 321-325.
Waga, D.D.O. 2007. The Paleocene-Eocene nannoplankton of theEast European Platform: Paleontology and Stratigraphy.
PhD thesis, Nation. Acad. of Science of Ukraine, Inst. ofGeol. Sciences, Kiev: 268pp.

Abstracts

125Electronic nannoplankton, version #4: a demonstration
Sherwood W. Wise, Jr., Matthew Olney, Mitchener Covington, Theodore Bibby,
Victoria M. Egerton, Shijun Jiang, Denise Kulhanek, Sarah Ramdeen, Patricia
A. Sims, Audra Wood, Alexander Davis, David R. Davenport, Nicole Doepler,
William Falcon, Carlos Lopez, C. T. Pressley, Hans M. Schrader, Olivia Swedberg, David M. Harwood & many others
Since its release at INA9 in Parma, Italy, INA CD-ROM
Series, No. 1, then entitled Electronic Calcareous Nannofossils, has sold out with some 150 copies distributed. Allproceeds go to the INA. The original motivation behind the
product was to provide an electronic package that could be
used by micropaleontologists at sea and in remote locations
such as Antarctica and elsewhere where hard-copy literature resources are limited. As such, various versions havebeen used aboard the Integrated Ocean Drilling Program’s
JOIDES Resolution for the past 15 years, and additional
databases have been added (see descriptions below in Wiseet al., 2002, 2003, 2004). The product is now used as wellfor classroom teaching and by industry professionals, including lab-based or well-site paleontologists making or
refining taxonomic identifications at the microscope. Theinteractive databases are displayed via a custom software
program called BugCam written in Visual Basic for use on
PCs. No other program is needed to run the databases,
hence they are stand-alone, self-contained packages as provided on the CD.
Version 4 will be released and demonstrated at INA12
in Lyon, France. In addition to the packages and databases
already incorporated in previous versions, it will include
the prototype of an interactive electronic database for
Cenozoic Antarctic Marine Diatoms (called ‘DiatomWare’)
along with a bibliography for that literature. Diatom specialists have long noted that their fossils also extend down
into the ‘nanno’ size range, hence we are pleased to accommodate them with the inclusion of this database on thislatest NannoWare CD. Over 500 taxa, grouped into 23 families or ‘family groups’ and 105 genera are included to datein DiatomWare, which has been described in some detailalong with a picture of the interface by Wise et al. (2007).
Biogeographic coverage lies within the present-day Southern Ocean, extending from the interior seas and continental shelves of Antarctica to the deep sea as far north as the
Subtropical Front, which separates surface waters originating in the tropics from those of Antarctic origin.
Holders of the earlier Versions 1, 2, or 3 of Electronic
Calcareous Nannofossils may exchange them through theTreasurers of the INA for Version 4 without charge. Copiesof these earlier versions received in exchange will be madeavailable with the compliments of the INA to individuals
and institutions that have not been able to meet the purchase price.

References
Wise, S.W., Covington, J.M., Ladner, B.C. & Wei, W. (Compilers)
2002. Electronic Calcareous Nannofossils, Version 1. International Nannoplankton Association, CD-ROM Series, No.
1. [Several databases plus the NannoWare/BugCam package,an interactive, icon-driven digital-image catalog of over 600
Cenozoic taxa authored by Wise, S.W., Bybell, L.M, Covington, J.M., de Kaenel, E., Maiorano, P. et al.]Wise, S.W., Covington, J.M., Ladner, B.C. & Wei, W. (Compilers)
2003. Electronic Calcareous Nannofossils, Version 2. International Nannoplankton Association, CD-ROM Series, No.
1. [As above, but with the addition of the Calcareous Nannoplankton Taxonomic Index (in 3 parts), scanned as necessary
and converted to MS Excel format by J. Ford, R. Hartman, J.
Lara, V. Regalado & A. Stant]Wise, S.W., Covington, J.M., Ladner, B.C. & Wei, W. (Compilers)
2004. Electronic Calcareous Nannofossils, Version 3. International Nannoplankton Association, CD-ROM Series, No.
1. [As above, but with the addition by several teams of contributors of Modern NannoWare (an interactive digital-image
catalog); The Consolidated Calcareous Nannoplankton Taxonomic Index in MS Excel Format; The Consolidated INA
Calcisphere Taxonomic Index in MS Excel Format; Augmented Cenozoic and Mesozoic Calcareous Nannoplankton
Bibliography [over 10 000 entries, and The Silicoflagellate
Bibliography]
Wise, S.W., Olney, M., Covington, J.M., Egerton, V.M. Jiang, S.,
Kulhanek, D.K., Ramdeen, S., Schrader, H.J., Sims, P.A.,
Wood, A.S., Davis, A., Davenport, D.R., Doepler, N., Falcon,
W,. Lopez, C., Pressley, T., Swedberg, O.L. & Harwood, D.M.
2007. Cenozoic Antarctic DiatomWare/BugCam: An aid forresearch and teaching. In: A.K. Cooper & C.R. Raymond etal. (Eds). Antarctica: A Keystone in a Changing World – Online Proceedings of the 10th ISAES, USGS Open-File Report
2007-1047, Short Research Paper, 017: 4pp. doi:
10.3133/of2007-1047.srp017.

126

Advertisement

Nannotax
www.nannotax.org
Nannotax is a website being developed to allow online documentation of nannofossil taxonomy,
broadcasting of images of nannofossils, and comment on them.
It uses the content management system Drupal, as
implemented within EDIT (European Distributed Instituteof Taxonomy), as a Taxonomy Information System - Scratchpads. The strengths of this system are that diverse information
can be uploaded and dynamically linked to individual taxa
(i.e. it can grow organically), that the commenting systemallows users to readily share their own observations, and that
contributors can edit and add to the content.

Or rather, this sort of web 2.0 accessibility is what thestrength of the site is intended to be. So far, there has not beenmuch uptake on the participation side, although there has
been a lot of good feedback. So, the main strength at present
is that the system has allowed me to develop, relatively
rapidly, a useful online guide to Neogene nannofossils.

The site contains pages for all the well-established Neogene
species, using the taxonomy from Young (1998). For eachspecies, there are currently brief descriptions and othercomments, together with a varying number of images.
Linking the species pages are pages on the higher taxa, withlonger descriptions, and tabular guides to the next level inthe taxonomy. Hopefully, the site can already be used, both asa reference source for experienced workers and as a tool forlearning nannofossil taxonomy. There is a lot of potential fordeveloping the site, including extending the coverage in termsof taxa and including additional content on the species.

I look forward to discussing it at INA12 (Lyon)
or why not get online, and start the taxonomic discussion now?!

Jeremy YoungAbstracts

Nannotax - a web-based system for documenting
nannofossil taxonomy
Jeremy R. Young
I have recently established an online guide to nannofossil
taxonomy using the content management system DruPal.
This has been facilitated by IT support from the European
Distributed Institute of Taxonomy (EDIT) project, and byencouragement from many colleagues especially Mike
Styzen (Shell) and the site is supported/endorsed by the
INA and the Gulf Coast section of SEPM.
The prime objective of the current phase ofdevelopment of the Nannotax site was to produce an online
version of Young (1998) - the Neogene chapter ofCalcareous Nannofossil Biostratigraphy. This has beensuccessfully achieved and the site is a useful demonstrationof the potential for a site covering a wider range ofnannofossil taxa. In this talk, I will demonstrate the current
state of the Nannotax system, show how users cancontribute to it, and discuss the potential for expansion.
References
Young, J.R. 1998. Neogene. In: P.R. Bown (Ed.). Calcareous
Nannofossil Biostratigraphy. British MicropalaeontologicalSociety Publications Series. Chapman & Hall, London: 225265.

127

128

Abstracts

The complex discovery of coccolithophores, from Ehrenberg
to Lohmann via Sorby, Wallich and Huxley
Jeremy R. Young
Coccolithophores are the smallest of routinely studied microfossils, only a few microns in diameter, in consequence
the nineteenth century history of their study is not a tale ofdedicated descriptive work by heroic pioneers. Instead it is
a complex history of slow discovery and controversy, involving many of the greatest microscopists of the era. It isin part a well-documented story, with different aspects
being covered by Gould (1978), Rehbock (1975), Rice etal. (1975), Rupke (1976) and Siesser (1994), especially asa result of the Bathybius controversy. However, re-examination of original material and manuscripts allows new perspectives to be given.
Like many other microfossils, coccoliths and discoasters were first described by the ‘founder of micropalaeontology’ Christian Gottfried Ehrenberg, and they are figured
in many of the plates of his magnum opus Mikrogeologie(Ehrenberg, 1854). However, they were at the limit of resolution of his microscopes and he regarded them as inorganic precipitates – kalk-morpholithien and crystalldrusen.
Subsequently, they were rediscovered in ocean bottom sediments by Thomas Huxley (1858), who coined the name‘coccolith’ for them on the basis of fine experimental observations that they were calcareous (hence ‘–lith’), and arather less impressive misinterpretation of them as spherical structures similar to ‘Protococcus’ cells (hence ‘Cocco’). He also sent some of the sediment to Henry Clifton
Sorby, the founder of petrographic microscopy. Sorby had
previously observed that the chalk is largely composed of
Ehrenberg’s calc-morpholiths and had inferred that they
were organic in origin. He rapidly established (Sorby,
1861) that Huxley’s coccoliths were the same as Ehrenbergs calc-morpholiths, and so that deep-sea oozes provided an analog for the chalk.
The story then gets complex, as agglutinating
foraminifera and inorganic precipitates lead the prime protagonists Wallich (a retired army doctor with scientific ambitions) and Huxley to infer that coccoliths were formedby the larvae of foraminifera (Wallich, 1861) or by a primordial slime covering the entire ocean bottom – Bathybius haeckelii (Huxley, 1868). The latter theory sounds like
implausible fantasy, but in fact stemmed from predictionsof Lorenz Okel, and especially Haeckel, and it briefly became a major scientific discovery, before being debunked
by the observations of the Challenger expeditions’ shipboard scientists in 1875. In parallel, Wallich became increasingly embittered at the lack of recognition of his
contributions; his annotated reprint collection, archived in
the NHM, provides spectacular evidence of his multiple
grievances. Nonetheless, he first demonstrated that coccoliths are components of coccospheres (a term he coinedin 1861) and, rather belatedly (Wallich, 1877), he documented that coccospheres were planktonic and described

the first two species – Coccosphaera pelagica and C. carteri. However, the numerous nineteenth century publications on coccoliths did little beyond establishing their basic
nature. The first truly heroic study of them only occurred in
the early twentieth century, with the remarkable work ofHans Lohmann, who coined the terms coccolithophore andnannoplankton, identified them as a major component of
the phytoplankton, developed techniques for sampling
them, and documented their taxonomy and biogeography(Lohmann, 1902, 1919).
References
Ehrenberg, C.G. 1854. Mikrogeologie: Das Erden und Felsen
schaffende Wirken des unsichtbar kleinen selbständigenLebens auf der Erde. Leopold Voss, Leipzig.
Gould, S.J. 1978. Bathybius meets Eozoon. Natural History,
87(4), 16-22. [Reprinted in The Panda’s Thumb: More Reflections in Natural History, 1980]
Huxley, T. 1858. Appendix A. In: J. Dayman (Ed.). Deep sea
soundings in the North Atlantic Ocean between Ireland and
Newfoundland made in H.M.S. Cyclops. The Admiralty Commissioners, London: 63-68.
Huxley, T.H. 1868. On some organisms living at great depths in
the North Atlantic Ocean. Quarterly Journal of Microscopical Science, 8: 203-212.
Lohmann, H. 1902. Die Coccolithophoridae, eine Monographie
der Coccolithen bildenden Flagellaten, zugleich ein Beitragzur Kenntnis des Mittelmeerauftriebs. Archiv für Protistenkunde, 1: 89-165.
Lohmann, H. 1919. Die Bevölkerung des Ozeans mit Plankton
nach den Ergebnissen des Zentrifugenfänge während der Ausreise der “Deutschland” 1911. Zugleich ein Beitrag zur Biologie des Atlantischen Ozeans. Archiv für Biontologie, 4(3),1-617.
Rehbock, P.F. 1975. Huxley, Haeckel and the oceanographers: thecase of Bathybius haeckelii. Isis, 66(4): 504-533.
Rice, A.L., Burstyn, H.L., Jones, A.G.E. 1976. G.C. Wallich M.D.
- Megalomaniac or mis-used oceanographic genius? Journalof the Society for the Bibliography of Natural History, 7(4):423-450.
Rupke, N. 1976. Bathybius haeckelii and the psychology of scientific discovery. Studies in the History and Philosophy of
Science, 7: 53-62.
Siesser, W.G. 1994. Historical background of coccolithophorestudies. In: A. Winter & W.G. Siesser (Eds).
Coccolithophores. Cambridge University Press, Cambridge:
1-11.
Sorby, H.C. 1861. On the organic origin of the so-called crystaloids of the chalk. Annals and Magazine of Natural History,
8: 193-200.
Wallich, G.C. 1861. Remarks on some novel phases of organic
life, and on the boring powers of minute annelids, at great
depths in the sea. Annals and Magazine of Natural History, 8:52-58.
Wallich, G.C. 1877. Observations on the coccosphere. Annals andMagazine of Natural History, 19: 342-350.

Abstracts

129

The role of coccolithophores in dimethylsulphide production
and their potential impact on climate
Jeremy R. Young, Dan Franklin, Gill Malin, Alex Poulton, Ian ProbertCharlson et al. (1987) noted that cloud formation over theoceans is significantly influenced by the supply of cloud
condensation nuclei, the predominant source of which appeared to be dimethylsulphide (DMS), which is producedby planktonic algae in sea water. Hence, increased phytoplankton productivity is liable to increase cloud cover andso global albedo. This system, commonly termed the
CLAW hypothesis, was envisaged as acting as a significant
negative feedback to the global warming effects of changed
insolation regimes and so as a partial global thermostat.
Subsequent research and modeling has confirmed the importance of DMS as a source of CCN, especially in theSouthern Hemisphere, indeed potential global temperature
impacts of up to 3.8 degrees centigrade have been calculated (Watson & Liss, 1998). However, research and modeling since Charlson (1987) has also shown that the system
is more complex and harder to predict than initiallythought. Indeed, it is not even clear whether the effect islikely to act as a positive or negative feedback to anthropogenic global change.
Complicating factors include that DMS is produced
from a precursor molecule dimethylsulphoniopropionate(DMSP), and the pathway from intracellular DMSP to atmospheric DMS is convoluted, with strong influences fromthe food-chain dynamics. Moreover the DMSP content ofphytoplankton varies greatly between species (Keller et al.,1989). Presumably as result of these two factors, there isoften only a poor correlation between phytoplankton biomass or productivity and DMS levels.
The pioneering work of Keller et al. (1989) suggested
that coccolithophores and dinoflagellates had much higher
DMSP contents than other phytoplankton, especially diatoms. Hence it is possible that varying abundances ofthese phytoplankon groups may be a significant factor controlling DMS production. To test this we have carried out
a combination of laboratory and cruisework investigationsof the role of coccolithophores in DMS production. The
laboratory investigations looked at variability in cellular
DMSP content across the phylogenetic diversity of coccolithophores. This revealed a remarkably consistent pattern, with all coccolithophores maintaining similar
concentrations of DMSP in their cells, supporting the interpretation that it plays a key role in cellular physiology,
probably as a compatible solute. The cruise-based work
consisted of parallel investigation of phytoplankton populations and the DMS-DLA-DMSP system during a transect
through the Mauretanian upwelling system.
References
Charlson, R., Lovelock, J., Andreae, M. & Warren, S. 1987.
Oceanic phytoplankton, atmospheric sulphur, cloud albedo
and climate. Nature, 326: 655-661.

Keller, M.D., Bellows, W.K. & Guillard, R.R.L. 1989. Dimethyl
sulphide production in marine phytoplankton. In: E.D. Saltzmann & W.J. Cooper (Eds). Biogenic sulfur in the environment. ACS Symposium Series No. 393: 167-182.
Watson, A.J. & Liss, P.S. 1998. Marine biological controls on
climte via the carbon and sulphur geochemical cycles. Philosophical Transactions of the Royal Society of London, B353:
41-51.

130

Abstracts

Adaptation of coccolith calcification to sea-water carbonate
chemistry
Patrizia Ziveri, Gerald Langer, Ian Probert, Jeremy Young
Coccolithophores are major calcifiers and through calcification cause feedbacks to atmospheric CO2 cycling. The
formation of CaCO3 in seawater, in fact, causes a shift ofthe carbonate system towards CO2, which in turn affects
atmosphere/ocean CO2 exchange. A change in marine calcification provides a concomitant feedback in organic carbon export and would lead to a change in the drawdown ofatmospheric CO2.
Coccolithophore culture experiments and field observations showed controversial results regarding the responseof calcification to high CO2. The three strains of Emiliania
huxleyi (the most abundant living coccolithophore species)
tested so far show both increased and decreased calcification at high CO2 levels (lower pH).
Living E. huxleyi is known to have a large variability inboth size and degree of calcification content, resulting invery large variation in coccolith mass, from about 1 to 5
pg. Recent field observations have suggested that the distribution of E. huxleyi coccolith morphotypes is related tocarbonate saturation state, even though the morphotypes
are known to be under strong genotypic control. This hypothesis can be tested by comparing the morphology of
coccolith strains, and especially their degree of calcification, with the sea-water carbonate chemistry from which
they were isolated. We selected 25 strains of E. huxleyi
maintained at the Roscoff culture collection, collected fromdifferent oceanographic settings with different carbon speciation. Although the strains are maintained at similar temperature and carbonate chemistry, they still preserve amorphology similar to the one of the original ocean samples. The selected strains have been grown at the same carbonate chemistry. The culture temperatures mimicked thetemperatures of the sites from where the strains were collected. With these experiments, we test the importance ofthe calcification strain adaptation to carbonate chemistry.
Size and possibly different responses to carbonate chemistry variations will also be discussed.

Addresses

131

INA12 authors’ addresses
Fatima Abrantes - Dept. of Marine Geology, INETI, 2720
Alfragide, Amadora, Portugal
Claudia Agnini - Dipt. di Geoscienze, Via Giotto, 1, 35137
Padova, Italy
F. Aguirre-Bahena - Centro Interdisciplinario de Ciencias
Marinas, Inst. Politécnico Nacional, México
Javier Alcántara-Carrió - Inst. de Investigación en Medio
Ambiente y Ciencia Marina, Univ. Católica de Valencia, 46003
Valencia, Spain; javier.alcantara@ucv.esBelén Alonso - Inst. de Ciencias del Mar (CSIC), Passeig Marítim
de la Barceloneta, 37-49, E-08003 Barcelona, Spain;
belen@icm.csic.es
M. Carmen Álvarez - Inst. de Investigación en Medio Ambiente
y Ciencia Marina, Universidad Católica de Valencia, 46003
Valencia, Spain; carmen.alvarez@ucv.es
Cleber Fernandes Alves - Fundação Gorceix/Petrobras, CENPES,
BrazilDavid Amblas - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Aida Sergeivna Andreeva-Grigorovich - Inst. of Geosciences,
Academy of Sciences of Ukraine, Kiev-54, 01054, Gonchara
Street 55b, Kiev, Ukraine
Gloria Andreini - Dipt. di Scienze della Terra, Univ. di Perugia,
Italy
Harald Andruleit - Bundesanstalt für Geowissenschaften &Rohstoffe, Stilleweg 2, D-30655 Hannover, Germany;h.andruleit@bgr.de
Alessandra Asioli - ISMAR, Consiglio Nazionale delle Ricerche,
Via Gobetti 101, I-40129 Bologna, Italy
Marie-Pierre Aubry - Dept. of Geology, Rutgers Univ., 610
Taylor Road, Piscataway, New Jersey, USA
Lia Auliaherliaty - Dept. of Paleoclimatology & Geomorphology, Fac. of Earth & Life Sciences, Vrije Univ. Amsterdam, De
Boelelaan 1085, 1081HV, Amsterdam, The Netherlands
Valia Avgoustidi - Hellenic Centre for Marine Research, Inst. of
Oceanography, 19013 Anavyssos, Greece
F. Azzaro - IAMC-CNR, U.O. di Messina, Italy
Jan Backman - Dept. of Geology & Geochemistry, Stockholm
Univ., SE-106 91 Stockholm, Sweden
T. Bahri - FAO MedSudMed Project, Roma, Italy
Ramona Balc - Babes-Bolyai Univ., Fac. of Biology & Geology,
Dept. of Geology, 1 Kogalniceanu St., Cluj-Napoca, 400084, Romania
Barbara Balestra - Dipt. di Scienze della Terra, Via G. La Pira 4,
50121 Firenze, Italy
Anne-Marie Ballegeer - Dept. de Geología, Univ. de Salamanca,
37008 Salamanca, Spain; amballegeer@usal.es
M. Ángeles Barcena - Univ. de Salamanca, Dept. de Geología,
Fac. de Ciencias, 37008 Salamanca, Spain; mbarcena@usal.es
Milos Bartol - Ivan Rakovec Inst. of Paleontology, ZRC SAZU,
Novi trg 2, PO Box 306, 1001 Ljubljana, Slovenia
Gretta Bartoli - Geological Inst., ETH Zürich, Universitätstraße
6, CH-8092 Zürich, Switzerland; gretta.bartoli@erdw.ethz.ch
G. Basilone - IAMC-CNR, U.O. di Mazara del Vallo, Italy
François Baudin - Univ. Pierre et Marie Curie, Paris 6 & UMR
7072 Tectonique, CNRS, CP 117, 4 Place Jussieu, 75252 Paris,
Cedex 05, France
Karl-Heinz Baumann - Dept. of Geosciences, University of Bremen, Klagenfurterstr., 28334 Bremen, Germany; baumann@uni-

bremen.de
Luc Beaufort - CEREGE, CNRS & Aix-Marseille Univ., Aix en
Provence, France
Ana Bento - Dept. of Geology, Fac. of Sciences, Univ. of Lisbon,
Campo Grande, 1749-016 Lisbon, Portugal
James Bergen - BP America, 200 West Lake Park Blvd., Houston,
TX 77079, USA
Gilen Bernaola - Dept. of Mining & Metallurgic Engineering,
Univ. of the Basque Country, E-48901 Barakaldo, Spain
Serge Berné - Géosciences Marines, IFREMER, BP 70, 29280
Plouzané, France
Adele Bertini - Dipt. di Scienze della Terra, Univ. degli Studi diFirenze, Via G. La Pira 4, 50100, Firenze, Italy
Theodore Bibby - Dept. of Geological Sciences, Florida State
University, Tallahassee, FL 32306-4100, USA
Teodora Blaj - Dept. of Geology & Geochemistry, Stockholm
Univ., SE-106 91 Stockholm, Sweden; teodora@geo.su.se
Babette Boeckel - FB5 Geowissenschaften, Universität Bremen,
Klagenfurterstr., 28359 Bremen, Germany
Ana-Voica Bojar - Karl-Fränzens Univ., Inst. für Erdwissenschaften, 26 Heinrichstraße, A-8010 Graz, Austria; anavoica.bojar@uni-graz.at
Jörg Bollmann - Geology Dept., Univ. of Toronto, Canada
A. Bonanno - IAMC-CNR, U.O. di Mazara del Vallo, Italy
Sergio Bonomo - Univ. di Palermo, Dipt. di Geologia e Geodesia,
Via Archirafi 22, 90134 Palermo, Italy & IAMC-CNR, U.O. di
Mazara del Vallo, Italy
David Bord - Dept. of Earth & Planetary Sciences, Rutgers Univ.,USA
Cinzia Bottini - Dept. of Earth Sciences, Univ. of Milan, Milan,
Italy; cinzia.bottini@unimi.it
Andrew R. Bowman - StatoilHydro, INT GEX GOM Regional
Team, 2103 CityWest Boulevard, Houston, TX 77042, USA
Paul R. Bown - Dept. of Earth Sciences, Univ. College London,
Gower Street, London, WC1E 6BT, UK
Vanda Brotas - Dept. Veg. Biology, Fac. of Sciences, Univ. of
Lisbon, Campo Grande 1749-016, Lisboa, Portugal
Colin Brownlee - Marine Biological Association, The Laboratory, Citadel Hill, Plymouth, PL1 2PB, UK
Margarita Buitrago-Reina - Dept. de Geología, Univ. de
Salamanca, Plaza de la Merced s/n, 37008 Salamanca, Spain:
margaritab@usal.es
G. Buscaino - IAMC-CNR, U.O. di Mazara del Vallo, Italy
Andrea Caburlotto - Ist. Nazionale di Oceanografia e diGeofisica Sperimentale, Trieste, Italy
Mário Cachão - Centre for Geology, Univ. of Lisbon, 1749-016
Lisboa, Portugal & Dept. of Geology, Fac. of Sciences, Univ. of
Lisbon, Campo Grande, 1749-016 Lisboa, Portugal;
mcachao@fc.ul.pt
Isabel Cacho - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Antonio Calafat - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Angelo Camerlenghi - ICREA, c/o GRC Geociències Marines,
Universidad de Barcelona, 08028 Barcelona, Spain
Miquel Canals - GRC Geociències Marines, Univ. de Barcelona,
08028 Barcelona, Spain
Damien Carcel - UMR CNRS 5125 PEPS, Univ. Claude Bernard,
Lyon 1, 69622 Villeurbanne cedex, France
Jose Luis Casamor - GRC Geociències Marines, Universidad de132

Addresses

Barcelona, 08028 Barcelona, Spain
Cristina Emanuela Casellato - Dipt. di Scienze della Terra‘A.Desio’, Univ. degli Studi di Milano, Italy
Simona Cavagna - Dipt. di Scienze della Terra, Univ. di Torino,
Via V. Caluso 35, 10125 Torino, Italy
James E.T. Channell - Dept. of Geological Sciences, Univ. of
Florida, Gainesville, Florida 32611, USA
Carmen Mariana Chira - Babes-Bolyai Univ., Fac. of Biology &Geology, Dept. of Geology, 1 Kogalniceanu St., Cluj-Napoca,
400084, Romania; mcchira@bioge.ubbcluj.ro
Abul Chrachri - Marine Biological Association, The Laboratory,
Citadel Hill, Plymouth, PL1 2PB, UK
Pierangelo Clari - Dipt. di Scienze della Terra, Univ. di Torino,
Via V. Caluso 35, 10125 Torino, Italy
Miriam Cobianchi - Dipt. di Scienze della Terra, Univ. degliStudi di Pavia, Via Ferrata 1, 27100 Pavia, Italy
Elena Colmenero-Hidalgo - Dept. de Geología, Univ. de
Salamanca, 37008 Salamanca, Spain & Dept. of Earth & Ocean
Sciences, Cardiff University, Cardiff, UK; elecolme@usal.es
Claude Colombié - UMR CNRS 5125 PEPS, Univ. Claude
Bernard Lyon 1, 69622 Villeurbanne cedex, France
María José Comas-Rengifo - Dept. y UEI de Paleontología, Fac.
de Ciencias Geológicas e Inst. de Geología Económica (CSICUCM), Calle José Antonio Novais, 2, 28040 Madrid, Spain; mjcomas@geo.ucm.es
Stjepan Coriç - Geological Survey of Austria, Neulinggasse 38,
A-1030 Vienna, Austria; stjepan.coric@geologie.ac.at
Mara Y. Cortés - Dept. Geología Marina, Univ. Autónoma deBaja California Sur, A.P. 19-B, CP 23080, La Paz, BCS, México;
mycortes@uabcs.mx
Sergio Costa - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Martine J.J. Couapel - CEREGE, Aix-Marseille Univ. CNRS,
IRD; Europôle Méditerrenéen de l’Arbois, BP80, 13545 Aix en
Provence, France
Mitchener Covington - BugWare, Inc., 4027 Bobbin Brook East,
Tallahassee, FL 32312, USALluïsa Cros - Inst. de Ciencias del Mar (CSIC), Passeig Marítim
de la Barceloneta, 37-49, E-08003 Barcelona, Spain;
lluisa@icm.csic.es
A. Cuttitta - IAMC-CNR, U.O. di Mazara del Vallo, Italy
David R. Davenport - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Alexander Davis - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Lúcia de Abreu - Godwin Lab., Univ. Cambridge, Cambridge,
CB2 3SA, UK
Bianca De Bernardi - Dept. of Earth Sciences ‘Ardito Desio’,
University of Milan, Milano, Italy
Mascha Dedert - Dept. of Paleoclimatology & Geomorphology,
FALW, Vrije Univ. Amsterdam, Amsterdam, The Netherlands;
dedm@falw.vu.nl
Eric de Kaenel - DeKaenel Paleo Research (DPR), Matile 51,
CH-2000 Neuchâtel, Switzerland & BP America, 200 West Lake
Park Blvd., Houston, TX 77079, USA
Francesco Dela Pierre - Dipt. di Scienze della Terra, Univ. di
Torino, via V. Caluso 35, 10125 Torino, Italy
Ben De Mol - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Bernard Dennielou - Géosciences Marines, IFREMER, BP 70,
29280 Plouzané, France
Anne de Vernal - Geotop, Univ. du Québec à Montréal, PO Box

8888, Montréal Qué, Canada, H3C3P8
Margarita D. Dimiza - Univ. of Athens, Fac. of Geology &Geoenvironment, Dept. of Historical Geology-Paleontology,
Panepistimiopolis 15784, Athens, Greece
Agata Di Stefano - Dipt. di Scienze Geologiche, Univ. of Catania,
Corso Italia 57, I-95129 Catania, Italy; distefan@unict.it
Enrico Di Stefano - Univ. di Palermo, Dipt. di Geologia e
Geodesia, Via Archirafi 22, 90134 Palermo, Italy
Nicole Doepler - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
O. Drebeka - Marine Biology Research Centre (MBRC), Tajura,
Libya
Luis Vitor Duarte - IMAR-CIC, Dept. de Ciências da Terra, Fac.
de Ciências e Tecnologia da Univ. de Coimbra, 3000-272
Coimbra, Portugal
Tom Dunkley Jones - Dept. of Geography, Univ. College London, Gower Street, London, WC1E 6BT, UK
Victoria M. Egerton - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Malte Elbrächter - Deutsches Zentrum für Marine
Diversitätsforschung,Forschungsinstitut
Senckenberg,
Wattenweerstation Sylt, Hafenstr. 43, DE-25992 List/Sylt, Germany
Elisabetta Erba - Dipt. di Scienze della Terra ‘A.Desio’, Univ.
degli Studi di Milano, Italy; elisabetta.erba@unimi.it
Gilles Escarguel - UMR 5125 PEPS, CNRS, Université Lyon 1,
Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Marta Estrada - Inst. de Ciències del Mar (CSIC), Passeig
Marítim, 37- 49, E-08003 Barcelona, Spain; marta@icm.csic.es
William Falcon - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Fereshte Farhad - Dept. of Earth Sciences, Shahid Beheshti
Univ., Tehran, IranRainer Feistel - Baltic Sea Research Inst., Seestrasse 15, DE18119 Warnemünde, Germany
Adrian Raymund C. Fernandez - National Inst. of Geological
Sciences, Univ. of the Philippines, Diliman, Quezon City 1101,
Philippines
Allan Gil S. Fernando - National Inst. of Geological Sciences,
Univ. of the Philippines, Diliman, Quezon City 1101, Philippines;
afernando@nigs.upd.edu.ph, braarudosphaera@yahoo.com
Christina Fink - Europrox, FB Geosciences, Univ. of Bremen,
PO Box 220440, 28334 Bremen, Germany; cfink@uni-bremen.deChiara Fioroni - Dipt. di Scienze della Terra, Univ. di Modena e
Reggio E., L.go S. Eufemia, 19, 41100 Modena, Italy
Florin Florea - Geomold, Campulung Moldovenesc, Romania
José-Abel Flores - Dept. de Geología, Univ. de Salamanca, Plazade la Merced s/n, 37008 Salamanca, Spain; flores@usal.esFrançois Fourel - UMR 5125 PEPS, CNRS, France; Univ. Lyon
1, Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, FranceÁngela Fraguas - Dept. y UEI de Paleontología, Fac. de Ciencias
Geológicas e Inst. de Geología Económica (CSIC-UCM), Calle
José Antonio Novais, 2, 28040, Madrid, Spain; arfragua@geo.ucm.es
Dan Franklin - Lab. for Global Marine & Atmospheric Chemistry, School of Environmental Sciences, Univ. of East Anglia,
Norwich, NR4 7TJ, UK
Conceição Freitas - Dept. of Geology, Fac. of Sciences, Univ. of
Lisbon, Campo Grande, 1749-016 Lisbon, Portugal

Addresses
Elke Freytag - FB5 Geowissenschaften, Univ. Bremen, Klagenfurterstr., 28359 Bremen, Germany
Jaume Frigola - GRC Geociències Marines, Univ. de Barcelona,
08028 Barcelona, Spain
Alessia Gadaleta - Dipt. di Scienze della Terra, Univ. di Parma,
V. Usberti, 157A, 43100 Parma, Italy
Ines Galoviç - Croatian Geological Survey, Sachsova 2, 10 000
Zagreb, Croatia; ingalovic@hgi-cgs.hr
Markus Geisen - Alfred Wegener Inst., Am Handelshafen 12,27570 Bremerhaven, Germany
Rainer Gersonde - Alfred Wegener Inst. für Polar- & Meeresforschung, Postfach 120161, D-27515 Bremerhaven, Germany
Fabienne Giraud - UMR CNRS 5125 PEPS, Univ. Claude
Bernard Lyon 1, 69622 Villeurbanne cedex, France
Larisa Golovina - Geological Inst., Russian Academy of Sciences, Moscow, Russia
Felix M. Gradstein - Museum of Natural History, University ofOslo, PO Box 1172 Blindern, N-0318 Oslo, Norway
José M. Gravalosa - Dept. de Geología, Univ. de Salamanca,
37008 Salamanca, Spain
Joan O. Grimalt - Dept. de Química Ambiental, Inst. deInvestigaciones Químicas y Ambientales (IIQAB-CSIC), 08034Barcelona, Spain
Darren Gröcke - Dept. of Earth Sciences, Durham Univ., Science
Labs, Durham, DH1 3LE, UK
Mauricio Grossi - Ist. Nazionale di Oceanografia e di Geofisica
Sperimentale, Trieste, Italy
Vincent Grossi - UMR 5125 PEPS, CNRS, France; Univ. Lyon 1,
Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Francis Grousset - CNRS, UMR 5805 EPOC, Univ. Bordeaux I,
Ave. des Facultés, Talence, 33405 France; f.grousset@epoc.ubordeaux1.fr
Fatemeh Hadavi - Geology Dept., Ferdowsi Univ. of Mashhad,
Mashhad, IranKyoko Hagino - Dept. of Natural History Sciences, Hokkaido
Univ., N10W8, Kita-ku, Sapporo, 060-0810 Japan & currently
Inst. for Study of Earth’s Interior, Okayama Univ., 827 Yamada,Misasa, Tottori, 682-0193 JapanEva Halásová - Dept. of Geology & Palaeontology, Fac. of Natural Sciences, Comenius Univ., Mlynská dolina G-1, 842 15
Bratislava, Slovak Republik; halasova@fns.uniba.sk
I.R. Hall - Dept. of Earth & Ocean Sciences, Cardiff Univ.,
Cardiff, UK
P.R. Halloran - Dept. of Earth Sciences, Univ. of Oxford, Oxford, UK
Till J.J. Hanebuth - Univ. Bremen, Fac. of Geosciences, PO Box
330440, 28334 Bremen, Germany
David M. Harwood - Dept. of Geosciences, Univ. of NebraskaLincoln, Lincoln, NE 68588-0340, USA; dharwood1@unl.edu
Jorijntje Henderiks - Dept. of Geology & Geochemistry, Stockholm Univ., Svante Arrheniusväg 8C, SE-106 91 Stockholm,
Sweden; jorijntje.henderiks@geo.su.se
Sandra Herrmann - Geological Inst., ETH Zürich, Universitätstraße
6,
CH-8092
Zürich,Switzerland;sandra.herrmann@erdw.ethz.ch
Johann Hohenegger - Dept. of Palaeontology, Univ. of Vienna,
Althanstrasse 14, A-1090 Vienna, Austria; johann.hohenegger@univie.ac.at
Takeo Horiguchi - Dept. of Natural History Sciences, Hokkaido
Univ., N10W8, Kita-ku, Sapporo, 060-0810 Japan133

Olaia Iglesias - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Alin Igritan - Babes-Bolyai Univ., Fac. of Biology & Geology,
Dept. of Geology, 1 Kogalniceanu St., Cluj-Napoca, 400084, Romania
Alessandro Incarbona - Univ. di Palermo, Dipt. di Geologia e
Geodesia, Via Archirafi 22, 90134 Palermo, Italy
Andrea Irace - CNR, Ist. di Geoscienze, Via V. Caluso 35, 10125
Torino, Italy
Marin Ivanov - Sofia Univ. ‘St. Kliment Ohridsky’, Fac. of Geology & Geography, 15 Tsar Osvoboditel Blvd., BG-1000 Sofia,
Bulgaria
Shijun Jiang - Dept. of Geological Sciences, Florida State Univ.,
Tallahassee, FL 32306-4100, USA
Haiyan Jin - State Key Lab. of Marine Geology, Tongji Univ.,
Shanghai 200092, PR China
Richard W. Jordan - Dept. of Earth & Environmental Sciences,Fac. of Science, Yamagata Univ., 1-4-12 Kojirakawa-machi, Yamagata 990 8560, Japan
Elsa Jullien - CNRS, UMR 5805 EPOC, Univ. Bordeaux I, Ave.
des Facultés, Talence, 33405 France; e.jullien@epoc.ubordeaux1.fr
Doru Toader Juravle - Al. I. Cuza Univ., Iasi, B-dul Carol I, 20
Anoshiravan L. Kani - Geology Dept., Fac. of Earth Science,
Shahid Beheshty Univ., Tehran, IranAtsuko Kijima - Dept. of Earth & Environmental Sciences, Fac.
of Science, Yamagata Univ., 1-4-12 Kojirakawa-machi, Yamagata
990 8560, Japan
Eduardo Apostolos Machado Koutsoukos - Petrobras/CENPES,
Brazil
Eva Krasakopoulou - Hellenic Centre for Marine Research, Inst.
of Oceanography, 19013 Anavyssos, Greece
Denise Kulhanek - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Sara Lafuerza - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Marcos A. Lamolda - Dept. de Estratigrafía y Paleontología, Fac.
de Ciencias, Univ. de Granada, Avda. de Fuentenueva s/n, 18002
Granada, Spain; mlamolda@ugr.es
Gerald Langer - Inst. of Environmental Science & Technology(ICTA), Univ. Autònoma de Barcelona (UAB), Bellaterra, Spain& Alfred Wegener Inst. for Polar & Marine Research, Bremerhaven, Germany
Galderic Lastras - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Caroline Lavoie - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Jackie A. Lees - Dept. of Earth Sciences, Univ. College London,
Gower Street, London, WC1E 6BT, UK
M. Leonardi - IAMC-CNR, U.O. di Messina, Italy
Valia Lianou - Univ. of Athens, Fac. of Geology & Geoenvironment, Dept. of Historical Geology-Paleontology, Panepistimiopolis 15784, Athens, Greece
Christian Linnert - Ruhr-Univ. Bochum, Universitätsstr. 150,
44801, Germany; christian.linnert@rub.de
Camino Liquete - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Chuanlian Liu - State Key Lab. of Marine Geology, Tongji Univ.,
Shanghai 200092, PR China

134

Addresses

Carlos Lopez - Dept. of Geological Sciences, Florida State Univ.,
Tallahassee, FL 32306-4100, USA
Gatsby-Emperatriz López-Otálvaro - Dept. of Geology, Univ. of
Salamanca, Plaza de la Merced, S/N, C.P. 37008, Salamanca,
Spain; gatsbyemperatriz@usal.es
Francesca Lozar - Dipt. di Scienze della Terra, Univ. di Torino,
Via V. Caluso 35, 10125 Torino, Italy; francesca.lozar@unito.it
Renata G. Lucchi - GRC Geociències Marines, Univ. deBarcelona, 08028 Barcelona, Spain
Claudia Lupi - Dipt. di Scienze della Terra, Univ. degli Studi diPavia,
Via
Ferrata
1,
27100
Pavia,
Italy;
clupi@manhattan.unipv.it
Ken MacLeod - Dept. of Geological Sciences, Univ. of MissouriColumbia, Columbia, MO 65211, USA
Azam Mahanipour - Geology Dept., Fac. of Earth Science,
Shahid Beheshty Univ., Tehran, IranGill Malin - Lab. for Global Marine & Atmospheric Chemistry,
School of Environmental Sciences, Univ. of East Anglia, Norwich, NR4 7TJ, UK
Elisa Malinverno - Dept. of Geological Sciences & Geotechnologies, Univ. of Milano-Bicocca, 4, 20126 Milano, Italy
Nicoletta Mancin - Dipt. di Scienze della Terra, Univ. degli Studi
di Pavia, Via Ferrata 1, 27100 Pavia, Italy
A. Marini - IAMC-CNR, U.O. di Messina, Italy
Sara Marreco - Dept. of Veg. Biology, Fac. of Sciences, Univ.
Lisbon, Campo Grande 1749-016, Lisboa, Portugal
Edoardo Martinetto - Dipt. di Scienze della Terra, Univ. di
Torino, Via V. Caluso 35, 10125 Torino, Italy
Akmal M. Marzouk - Geology Dept., Fac. of Science, Tanta
Univ., Tanta 31527, Egypt; akmal_marzouk@hotmail.com
F. Massa - FAO MedSudMed Project, Roma, Italy
Emanuela Mattioli - UMR 5125 PEPS, CNRS, France; Univ.
Lyon 1, Campus de la DOUA, Bâtiment Géode, 69622
Villeurbanne Cedex, France
S. Mazzola - IAMC-CNR, U.O. di Messina, Italy
Helge Meggers - Dept. of Geosciences, Univ. of Bremen, Germany
Sebastian Meier - Christian Albrechts Univ. zu Kiel, Lab. fürRasterelektronenmikroskopie, Ludewig-Meyn-Straße 16, 24118
Kiel, Germany; smeier@gpi.uni-kiel.de
Alejandra Mejía-Molina - Univ. de Salamanca, Dept. deGeología, Fac. de Ciencias, Salamanca, 37008 Spain; alejandra@usal.es
Mihaela C. Melinte-Dobrinescu - National Inst. of Marine Geology & Geo-ecology, 23-25 Dimitrie Onciul Street, RO-024053
Bucharest, Romania; melinte@geoecomar.ro
Fab Minoletti - Univ. Pierre et Marie Curie, Paris 6; Lab. Biominéralisations & Paléoenvironnements (JE2477), T56-55 5eme Case 116, 4, Place Jussieu, 75252 Paris cedex 05, France
Alan C. Mix - College of Oceanic & Atmospheric Sciences, Oregon State Univ., Corvallis, Oregon, USA
Svetlana F. Mizintseva - Dept. of Earth & Planetary Sciences,
Rutgers Univ., Piscataway, NJ 08854, USA
Simonetta Monechi - Dipt. di Scienze della Terra, Via La Pira 4,
50121 Firenze, Italy
Jörg Mutterlose - Ruhr-Univ. Bochum, Universitätsstr. 150,
44801, Germany; joerg.mutterlose@rub.de
Giovanni Muttoni - Dipt. di Scienze della Terra ‘A.Desio’, Univ.
degli Studi di Milano, ItalyÁurea Narciso - Dept. of Geology, Fac. of Sciences, Univ. of Lisbon, Campo Grande, 1749-016 Lisbon, Portugal

Hiroshi Nishi - Division of Earth & Planetary Sciences, Graduate
School of Science, Hokkaido University, N10W8, Kita-ku, Sapporo 060-0810, Japan
Hisatake Okada - Division of Earth & Planetary Sciences, Graduate School of Science, Hokkaido University, N10W8, Kita-ku,
Sapporo 060-0810, Japan
Mathew Olney - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Silvia Palandri - Dipt. di Scienze della Terra, Univ. di Pisa, Via
S. Maria 53, 56126 Pisa, Italy
Stefano Palmerini - UMR 5125 PEPS, CNRS, France; Univ.
Lyon 1, Campus de la DOUA, Bâtiment Géode, 69622
Villeurbanne Cedex, France
Guido Parisi - Dipt. di Scienze della Terra, Univ. di Perugia, Italy
B. Patti - IAMC-CNR, U.O. di Messina, Italy
Laura Pea - Dipt. di Scienze della Terra, Univ. di Parma, V.
Usberti 157A, 43100 Parma, Italy
Maria Teresa Pedrosa - GRC Geociències Marines, Universidad
de Barcelona, 08028 Barcelona, Spain
Alyssa M. Peleo-Alampay - National Inst. of Geological Sciences, Univ. of the Philippines, Diliman, Quezon City, Philippines
Nicola Pelosi - Consiglio Nazionale delle Ricerche, Ist. perl’Ambiente Marino Costiero, Calata Porta di Massa, Interno Portodi Napoli, 80133 Naples, Italy
Nicola Perilli - Dipt. di Scienze della Terra, Univ. degli Studi diPisa, Via Santa Maria 53, 56100 Pisa, Italy; perilli@dst.unipi.it
Davide Persico - Dipt. di Scienze della Terra, Univ. di Parma, V.
Usberti 157A, 43100 Parma, Italy
Bernard Pittet - UMR 5125 PEPS, CNRS, France; Univ. Lyon 1,
Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Andrea Piva - ISMAR, Consiglio Nazionale delle Ricerche, Via
Gobetti 101, I-40129 Bologna, Italy
Julien Plancq - UMR 5125 PEPS, CNRS, France; Univ. Lyon 1,
Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Mirela Violetta Popa - Babes-Bolyai Univ., Fac. of Biology &Geology, Dept. of Geology, 1 Kogalniceanu St., Cluj-Napoca,
400084, Romania
Alex Poulton - National Oceanography Centre, Southampton,
SO14 3ZH, UK
Channarayapattana Prabhu - Centre for Marine & Environmental Research, 289, Porto, 4050-123 Portugal & Dept. of Marine
Geology, INETI, 2720 Alfragide, Amadora, Portugal
C.T. Pressley - Dept. of Geological Sciences, Florida State Univ.,
Tallahassee, FL 32306-4100, USA
Ian Probert - Station Biologique de Roscoff, 29682 Roscoff,FranceIsabella Raffi - Dipt. di Geotecnologie per l’Ambiente e il
Territorio, Univ. ‘G. d’Annunzio’ di Chieti-Pescara, Via dei
Vestini 31, 66013 Chieti, Italy
Naser Raisossadat - Geology Dept., Fac. of Science, Birjand, IranSarah Ramdeen - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Viviana Reale - Dipt. di Scienze della Terra, Univ. degli Studi diFirenze, Via G. La Pira 4, 50100, Firenze, Italy
Michele Rebesco - Ist. Nazionale di Oceanografia e di Geofisica
Sperimentale, Trieste, Italy
Letizia Reggiani - Dipt. di Scienze della Terra, Univ. degli Studi
di Perugia, Italy & UMR 5125 PEPS, CNRS, France; Univ. Lyon

Addresses
1, Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Frédéric Ricciardi - Total S.A., Dept. Biostratigraphy
R.E.M. Rickaby - Dept. of Earth Sciences, Univ. of Oxford, Oxford, UK
Stuart Robinson - Dept. of Earth Sciences, Univ. College London, Gower Street, London, WC1E 6BT, UK
Teresa Rodrigues - Dept. of Marine Geology, INETI, 2720
Alfragide, Amadora, Portugal
Olga M. Rodríguez V. - PDVSA E&P, Gerencia de LaboratoriosyNucleotecas,
PuertoLa
Cruz,
Venezuela;
rodriguezou@pdvsa.com
Björn Rost - Alfred-Wegener-Inst. for Polar & Marine Research,
Bremerhaven, Germany
Mariem Saavedra-Pellitero - Dept. de Geología, Univ. de
Salamanca, Plaza de la Merced s/n 37008, Salamanca, Spain;
mariemsaavedra@usal.es
Armando Antônio Scarparo Cunha - PETROBRAS/CENPES,
Rio de Janeiro, Brazil
Niels Schovsbo - Geological Survey of Denmark & Greenland(GEUS), Øster Voldgade 10, DK 1350, Copenhagen K, Denmark
Hans M. Schrader - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Ekaterina Shcherbinina - Geological Inst. of the Russian Academy of Sciences, Russia
Emma Sheldon - Geological Survey of Denmark & Greenland(GEUS), Øster Voldgade 10, DK 1350, Copenhagen K, Denmark
Seirin Shimabukuro - PETROBRAS/CENPES, Brazil
Anatoliy Shumnyk - Dept. of Geological Sciences, Florida State
Univ.,
Tallahassee,
FL
32306-4100,
USA;
anatoliy.shumnyk@bugware.com
Francisco Javier Sierro - Dept. de Geología, Univ. de Salamanca,
Plaza de la Merced s/n, 37008 Salamanca, Spain; sierro@usal.es
Norman Silverberg - Centro Interdisciplinario de Ciencias
Marinas, Inst. Politécnico Nacional, México
Débora Simón-Baile - Dept. de Geología, Univ. de Salamanca,
Plaza de la Merced s/n, 37008 Salamanca, Spain
Patricia A. Sims - Botany Dept., The Natural History Museum,
Cromwell Road, London, SW7 5BD, UK
Claudia Sprengel - Bundesanstalt für Geowissenschaften &Rohstoffe, Stilleweg 2, D-30655 Hannover, Germany
Mario Sprovieri - Consiglio Nazionale delle Ricerche, Ist. perl’Ambiente Marino Costiero, Calata Porta di Massa, Interno Portodi Napoli, 80133 Naples, Italy
Rodolfo Sprovieri - Univ. di Palermo, Dipt. di Geologia e
Geodesia, Via Archirafi 22, 90134 Palermo, Italy
Lars Stemmerik - Dept. of Geography & Geology, Copenhagen
Univ., Øster Voldgade 10, DK 1350, Copenhagen K, Denmark
Heather Stoll - Dept. de Geología, Univ. de Oviedo, Arias de Velasco, s/n 30005, 33005 Oviedo, Asturias, Spain & Geoscience
Dept., Williams College, Williamstown, MA 01267, USA
Katharina Stolz - EUROPROX - Univ. Bremen, Fac. of Geosciences, PO Box 330440, 28334 Bremen, Germany; kstolz@unibremen.de
Kristalina Stoykova - Geological Inst., Bulgarian Academy of
Sciences, 24 G. Bonchev Str., BG-1113 Sofia, Bulgaria
Gioconda Sturiale - Dipt. di Scienze Geologiche, Univ. of
Catania , Corso Italia 57, I-95129 Catania, Italy; gsturia@unict.it
Guillaume Suan - UMR 5125 PEPS, CNRS, Univ. Lyon 1,
Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Baptiste Suchéras-Marx - UMR 5125 PEPS, CNRS, Univ. Lyon

135

1, Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Finn Surlyk - Dept. of Geography & Geology, Copenhagen
Univ., Øster Voldgade 10, DK 1350, Copenhagen K, Denmark
Lilian Švábenická - Czech Geological Survey, Klárov 131/3, PO
Box
85,
118
21
Praha
1,
Czech
Republic;
lilian.svabenicka@geology.cz
Olivia Swedberg - Dept. of Geological Sciences, Florida State
Univ., Tallahassee, FL 32306-4100, USA
Yoshihito Takano - Inst. for East China Sea Research, Nagasaki
Univ., Nagasaki, Japan
Reishi Takashima - School of Marine & Resources, Tokai Univ.,
3-20-1, Orido, Shimizu-ku, Shizuoka, 424-8610, Japan
M. Talha - Marine Biology Research Centre (MBRC), Tajura,
Libya
Deborah N. Tangunan - National Inst. of Geological Sciences,
Univ. of the Philippines, Diliman, Quezon City, Philippines
Alison Taylor - Marine Biological Association, The Laboratory,
Citadel Hill, Plymouth, PL1 2PB, UK
Nicolas Thibault - Dept. of Geography & Geology, Copenhagen
Univ., Øster Voldgade 10, DK 1350, Copenhagen K, Denmark
Hans R. Thierstein - Geological Inst., ETH Zürich & Univ.
Zürich, Universitätstraße 6, CH-8092 Zürich, Switzerland;hans.thierstein@erdw.ethz.ch
Daniele Tiraboschi - Dept. of Earth Sciences, Univ. of Milan,
Milan, Italy; daniele.tiraboschi@unimi.it
Lucio Riogi Tokutake - PETROBRAS/UN-ES/EXP/SE, Espírito
Santo Sedimentology & Stratigraphy Sector, Brazil
Felipe Antonio de Lima Toledo - Lab. de Paleoceanografia doAtlântico Sul (LaPas), Inst. Oceanográfico (IO), Univ. de São
Paulo (USP), Brazil
Vladimir Torres Torres - Inst. Colombiano del Petróleo, ICP,ECOPETROL S.A., Km.7 vía Piedecuesta, Santander, Colombia;
vladimir.torres@ecopetrol.com.co
G. Tranchida - IAMC-CNR, U.O. di Mazara del Vallo, Italy
Iacopo Trattenero - Dipt. di Scienze della Terra, Univ. degli Studi
di Pavia, Via Ferrata 1, 27100 Pavia, Italy
Stefania Trenkwalder - CNR, Ist. di Geoscienze, Via V. Caluso
35, 10125 Torino, Italy
Maria V. Triantaphyllou - Univ. of Athens, Fac. of Geology &Geoenvironment, Dept. of Historical Geology-Paleontology,
Panepistimiopolis 15784, Athens, Greece
Francisco. J. Urcádiz-Cázares - Dept. Geología Marina, Univ.
Autónoma de Baja California Sur, A.P. 19-B, CP 23080, La Paz,
BCS, México
Roger Urgeles - GRC Geociències Marines, Universidad deBarcelona, 08028 Barcelona, Spain
Anja van der Plas - National Marine Information & ResearchCentre, PO Box 912, Swakopmund, Namibia
Giuliana Villa - Dipt. di Scienze della Terra, Univ. di Parma, V.
Usberti 157A, 43100 Parma, Italy
Donata Violanti - Dipt. di Scienze della Terra, Univ. di Torino, via
V. Caluso 35, 10125 Torino, Italy
Antje Voelker - Dept. of Marine Geology, INETI, 2720 Alfragide,
Amadora, Portugal
DennisDanielWaga
National
Enterprise‘NAUKANAFTOGAZ’, Kiev region, Vyshneve - 08132, Kievska
Street, 8, Russia; wagadennis@rambler.ru
Maria Dolores Wanderley - UFRJ, CCMN, Inst. de Geociências,

136

Addresses

Dept. de Geologia
David K. Watkins - Dept. of Geosciences, University of Nebraska, 214 Bessey Hall, Lincoln, NE 68588, USA
Andrew F. Weller - Geological Inst., ETH Zürich, Universitätstraße
6,
CH-8092
Zürich,Switzerland;
andrew.weller@erdw.ethz.ch
Glenn Wheeler - Marine Biological Association, The Laboratory,
Citadel Hill, Plymouth, PL1 2PB, UK
Amos Winter - Dept. of Marine Sciences, Univ. of Puerto Rico,
PO Box 9013, PR 00681-9013 Mayagüez, Puerto Rico
Monica Winsborrow - University of Tromsø, Dept. of Geology,
Tromsø, Norway
Sherwood S. Wise, Jr. - Dept. of Geological Sciences & the
Antarctic Marine Geology Research Facility, Florida State Univ.,
Tallahassee, FL 32306-4100, USA; wise@gly.fsu.edu
Audra Wood - Dept. of Geological Sciences, Florida State Univ.,
Tallahassee, FL 32306-4100, USA
George Yordanof - UMR 5125 PEPS, CNRS, France; Univ. Lyon
1, Campus de la DOUA, Bâtiment Géode, 69622 Villeurbanne
Cedex, France
Jeremy R. Young - Palaeontology Dept., The Natural History Museum, Cromwell Road, London SW7 5BD, UK
S. Zgozi - Marine Biology Research Centre (MBRC), Tajura,
Libya
Shiying Zhang - State Key Lab. of Marine Geology, Tongji Univ.,
Shanghai 200092, PR China
Patrizia Ziveri - ICTA, Universitat Autónoma de Barcelona(UAB), Edifici Cn - Campus UAB, 08193 Bellaterra, Spain &Dept. of Paleoclimatology & Geomorphology, Fac. of Earth &Life Sciences, Vrije Univ. Amsterdam, De Boelelaan 1085
1081HV, Amsterdam, The Netherlands