Preliminary stable oxygen isotope data are presented from the southern North Sea Basin successions, ranging from the Lutetian to Rupelian. Analyses were performed on fish otoliths, nuculid bivalves and benthic foraminifera and are presented as bulk delta(18)O values relative to a well established regional sequence stratigraphic framework. The most significant positive shift in delta(18)O values clearly falls at the top of the regionally recognised Bassevelde 3 sequence, which base corresponds to the Eocene-Oligocene GSSP boundary. The here documented delta(18)O shift is closely associated with the base of the traditional Rupelian unit-stratotype and is tentatively correlated to the globally recognised Oi-1 event

De Man, E.

Ivany, L.

Vandenberghe, N.

Open Marine Archive

Netherlands Journal of Geosciences / Geologie en Mijnbouw 83 (3): 193-197 (2004)
Netherlands Journal of Geosciences / Geologie en Mijnbouw 83(3) 2004 193
Stable oxygen isotope record of the Eocene-Oligocene transition
in the southern North Sea Basin: positioning the Oi-1 event 
E. De Man1, L. Ivany2 & N. Vandenberghe3
1 Royal Belgian Institute of Natural Sciences, Vautierstraat 29, B-1000 Brussels, Belgium 
Ellen.DeMan@naturalsciences.be (corresponding author)
2 Department of Earth Sciences, Syracuse University, Syracuse, New York 13244, USA
3 Historical Geology, K.U. Leuven, Redingenstraat 16, B-3000 Leuven, Belgium
Manuscript received: February 2004; accepted: August 2004
Abstract
Preliminary stable oxygen isotope data are presented from the southern North Sea Basin successions, ranging from the
Lutetian to Rupelian. Analyses were performed on fish otoliths, nuculid bivalves and benthic foraminifera and are presented
as bulk δ18O values relative to a well established regional sequence stratigraphic framework.The most significant positive shift
in δ18O values clearly falls at the top of the regionally recognised Bassevelde 3 sequence, which base corresponds to the
Eocene-Oligocene GSSP boundary. The here documented δ18O shift is closely associated with the base of the traditional
Rupelian unit-stratotype and is tentatively correlated to the globally recognised Oi-1 event.
Keywords: Eocene-Oligocene boundary, stable isotopes, Oi-1 event, sequence stratigraphy
Introduction
As a proxy for earth’s changing climate, δ18O curves
have been established for different regions all over the
world. At the Eocene-Oligocene transition, several
notable positive excursions in the curve have been
recognised, mostly based on data from the open ocean
(e.g., Zachos et al., 1996, 2001; Miller et al., 1991,
1998; Abreu & Anderson, 1998; Bohaty & Zachos,
2003). Beginning in the basal Oligocene, oxygen iso-
tope values of marine carbonates become significantly
more positive than those of the late Eocene.The earliest
and largest magnitude shift has been termed the Oi-1
event, and occurred between 33.5 and 33.05 Ma
(Zachos et al., 1996), slightly later than the Eocene-
Oligocene boundary at 33.7 Ma (Odin & Montanari,
1989). Although the primary cause of this δ18O shift
remains controversial (e.g., Lear et al., 2000), its global
character is widely accepted and can thus be applied
to resolve stratigraphic problems around that crucial
time interval.
The southern North Sea Basin (Fig. 1) is of particular
stratigraphic interest, because it is home of several
unit-stratotype sections of the Paleogene, such as the
Rupelian Stage which has been defined in the Boom
Formation in northern Belgium (Dumont, 1849).
Although the regional stratigraphic framework of this
region is well constrained, correlation to the inter-
national time scale is often hampered around the
Eocene-Oligocene interval because of the absence of
time-indicative calcareous index fossils. The base of
the Rupelian unit-stratotype has been correlated to
the Massignano section in central Italy by means of
organic walled dinoflagellate cysts (Stover &
Hardenbol, 1994; Brinkhuis & Visscher, 1995) and
proved to coincide with a level well above the Eocene-
Oligocene Global boundary Stratotype Section and
Point (GSSP).Vandenberghe et al. (2003) incorporated
Netherlands Journal of Geosciences / Geologie en Mijnbouw 83(3) 2004194
these results into a regional sequence stratigraphic
framework and indicated that the Eocene-Oligocene
GSSP correlates with a level between the Bassevelde 2
and Bassevelde 3 sequences, whereas the base of the
Rupelian unit-stratotype belongs to the younger
Boom sequence (see Fig. 2).
Isotopic studies on the North Sea Basin are limited
(e.g., Buchardt, 1978; Schmitz et al., 1996) and have
never been applied in stratigraphic problems for the
time interval discussed in this paper. The goal of this
preliminary study is to document the δ18O signal of
the Eocene-Oligocene deposits in the southern North
Sea Basin, compare it to the globally recognised Oi-1
event, and to evaluate its position in respect to the
Eocene-Oligocene GSSP and the regional sequence
stratigraphic framework.
Geological setting
During the terminal Eocene and transition to the
Oligocene, northern Belgium occupied the southern-
most part of the Cenozoic North Sea Basin (Fig. 1)
and today provides a well documented reference shelf
section for that time interval. The Lower Oligocene
Rupelian Stage has originally been defined in the stiff
clays cropping out along the river Rupel in northern
Belgium (Fig. 1), nowadays lithostratigraphically
referred to as the Boom Formation (Fig. 2). Recent
sequence stratigraphic studies distinguish four depo-
sitional sequences within the Eocene-Oligocene tran-
sitional interval (Bassevelde 1, 2 and 3 and Boom 1
sequence; NP18-NP23; Vandenberghe et al., 2003)
and interpret the Boom Formation as part of a second
BELGIUM
0 10 20 km
Rupel
Schelde
M
aa
s
5°E
51°N
C A
M P
I
E
N
S OUT
H
LIMB
U R G
60°N
0°
50°N
10°E 20°E10°W
N
N
A
outcrop area Boom Fm.
sections studied
major faults
major cities
HOBOKEN
TEMSE
EIGENBILZEN
VLIERMAAL
Gent
BALEGEM
Brugge
Luik
OEDELEM
KRUIBEKE
WEMMEL
RUMST
GRIMMERTINGEN
BRUSSELS
Mechelen
Leuven
Antwerpen
Hasselt
B
WEELDE
Fig. 1. A. Paleogeographic
map of northwest Europe
during Rupelian times. Shaded
areas indicate land, white areas
marine conditions. (Modified
after Ziegler, 1990; Sissingh,
2003). Coordinates represent
present day UTM coordinates.
B. Location of studied sections.
Netherlands Journal of Geosciences / Geologie en Mijnbouw 83(3) 2004 195
Oligocene sequence that starts at the base of the
underlying Ruisbroek Sand Member. The older
Bassevelde 3 depositional sequence hence makes up
the first Oligocene sediments within the North Sea
Basin. These insights result from detailed biostrati-
graphical correlations by means of dinoflagellates
(Stover & Hardenbol, 1994; Brinkhuis & Visscher,
1995), showing that the exact position of the Eocene-
Oligocene boundary as defined by the GSSP in
Massignano (Central Italy) falls at the base of the
Bassevelde 3 sequence, well below the base of the tradi-
tional Rupelian unit-stratotype (Fig. 2;Vandenberghe
et al., 2003).
The age of the North Sea Basin section is estab-
lished based on detailed bio- and sequence strati-
graphy, and is further constrained by magnetostrati-
graphic and geochemical anchor points (Stover &
Hardenbol, 1994; Brinkhuis & Visscher, 1995;
Vandenberghe et al., 2001, 2003; Van Simaeys et al.,
2004; Lagrou et al., 2004). Appropriate age data for
these anchor points as calibrated by Berggren et al.
(1995) are summarized in Fig. 2.
Fig. 2. Positioning of the Oi-1 isotope event of Zachos et al. (1996) within the southern North Sea Basin composite section, by calibration
with the Bohaty & Zachos (2003) oxygen isotope curve. Formations and Members that were sampled in this study are indicated in bold in
the composite section (CS). (*) marks the base of the traditional Rupelian Stage; note the discrepancy with the official Eocene-Oligocene
boundary GSSP.The Bassevelde 3 sequence corresponds to the marine tongrian deposits. Calcareous nannoplankton zonation for the lower
part of the section after Steurbaut (1992), for the upper part after Van Simaeys et al. (2004). A summary of all age calibration methods is
given in Van Simaeys et al. (2004) and dates are given according to Berggren et al. (1995).
Netherlands Journal of Geosciences / Geologie en Mijnbouw 83(3) 2004196
Materials and Methods
Fish otoliths (ear stones, mainly from the family
Congridae), nuculid bivalves (Nuculana deshayesiana),
and benthic foraminifera (Cibicidoides spp. and
nodosariids) from the above mentioned units were
selected for analysis from core and outcrop samples
in the southern North Sea Basin (Fig. 1) based on
their size and quality of preservation. Otoliths and
bivalves were sectioned and polished to reveal fresh
aragonite within, and sample trajectories were drilled
perpendicular to the axis of growth in pristine portions
of the structures with a Merchantek MicroMill so as
to subsume any intra-annual variation within the
sample and thereby derive overall average bulk
compositions.Three to five samples were collected in
this manner from each specimen. Benthic foraminifera
were prepared as in Thomas et al. (2000). Between 5
and 50 cleaned specimens from each sample were
crushed and pieces of test calcite selected for analysis.
Stable oxygen isotope analyses were performed on a
Finnigan MAT 251 mass spectrometer at the
University of Michigan Stable Isotope Laboratory,
and are reported relative to the VPDB standard.
56 fish otoliths, 14 nuculid bivalves, and 10 benthic
foraminiferan samples were analyzed for this initial
investigation. While otoliths provide the bulk of the
data upon which this present analysis is based, wher-
ever possible we have selected and sampled otolith,
bivalve, and foraminiferan carbonate from the same
sample horizons in order to enable the establishment
of inter-taxon calibrations for use in future compi-
lations. This will allow the extension of our record
into the subsurface using borehole samples domi-
nantly consisting of foraminifera, and across strati-
graphic intervals in outcrop where only one of the
three groups is present. In this manner, a more com-
plete geochemical record can be generated from the
middle Eocene through the Oligocene (De Man et
al., in preparation).
A composite section (CS) was constructed ranging
from the Middle Eocene to Lower Oligocene in order
to represent the sampled interval (Fig. 2). The corre-
lation between the fully marine sediments of the
Campine area (northern Belgium) and the more mar-
ginal marine sediments of the Limburg area (central
to northeast Belgium) is based on geophysical well
log correlation (Vandenberghe et al., 2001, 2003)
combined with calcareous nannoplankton (Steurbaut,
1992) and organic walled dinoflagellate (De Coninck,
2001) biostratigraphy. At present, no upper Eocene
samples are included due to a lack of available out-
crops; however we expect to remedy this deficiency
using borehole samples in future analyses.
Results and discussion
The resulting δ18O values from all taxa are plotted in
Fig. 2, relative to the VPDB standard. No correction
factors have yet been established and thus bulk data
are compared to fine fraction analyses of Bohaty &
Zachos (2003). Since no detailed curve has yet been
established for shelf sections for the studied interval
(Lutetian to Rupelian), our results are best compared
to δ18O variations within the surface waters of the open
ocean.
δ18O values show a clear distinction between the
middle Eocene and lower Oligocene samples, the
former ranging from –2.5‰ to –0.5‰ and the latter
from –0.5‰ to +1‰ (Fig. 2). The lowermost
Oligocene samples from the Grimmertingen Sands
(near-shore equivalent of Bassevelde 3 sequence, see
Vandenberghe et al., 2003, fig. 24.7) still show
prevailing low δ18O values, ranging from –2.5‰ to
–0.5‰. Hence, the main δ18O shift clearly falls above
the Bassevelde 3 sequence, near the base of the tradi-
tional Rupelian Stage (or second Oligocene deposi-
tional sequence according to Vandenberghe et al., 2003)
(Fig. 2). Seen the magnitude of the observed δ18O shift
(~1.5‰) and its stratigraphic position, it is believed to
correspond to the Oi-1 event observed in the open
ocean (comprising the Oi-1a and Oi-1b of Zachos et
al., 1996, Fig. 4, 6; Bohaty & Zachos, 2003).
It is unlikely that these results are biased toward
more negative values by either diagenesis or fresh-
water influx. The Grimmertingen Sands have not
suffered any significant diagenetic alteration, as shown
by the unconsolidated nature of the sands and the
preservation of original aragonite within the fossils. In
addition, the presence of glauconite clearly points
towards a marine origin of the sands, while the
enclosed fossils give evidence for shelf conditions well
below wave influence, away from potential estuarine
areas (Winkelmolen, 1972;Vandenberghe et al., 1998,
p. 141-144). Unless the entire basin suffered from
brackish conditions, it is unlikely that the negative
δ18O values can be explained by mixing with fresh
water. Geochemical evidence from δ13C or 86Sr/87Sr
is not yet available to unequivocally confirm these
findings, but will be considered in future initiatives.
Conclusions
Preliminary oxygen isotope data from the well cali-
brated southern North Sea Basin successions indicate
that the most significant positive shift in δ18O values
(correlated to the Oi-1 event of Zachos et al., 1996)
is situated well within the Oligocene if calibrated
against the Eocene-Oligocene GSSP. This study
Netherlands Journal of Geosciences / Geologie en Mijnbouw 83(3) 2004 197
proves that the Oi-1 event falls above the Bassevelde
3 sequence and is thus closely associated with the
base of the traditional Rupelian unit-stratotype.
Acknowledgements
Dirk Nolf is thanked for providing otolith samples
and helping with identifications. Many thanks go to
Lora Wingate for providing isotope analyses and to
Frans Moorkens for all-round technical support. We
are indebted to Stefaan Van Simaeys and Etienne
Steurbaut for fruitful discussions. Dr. Ellen Thomas
is gratefully acknowledged for a detailed review of the
paper. This work was supported by FWO-Flanders
(research grant G.0093.01). EDM acknowledges the
support of the DWTC-Brussels (Grant WI/36/C03).
References
Abreu, V.S. & Anderson, J.B., 1998. Glacial eustasy during the
Cenozoic: sequence stratigraphic implications. AAPG Bulletin,
82(7): 1385-1400.
Berggren, W.A., Kent, D.V., Swisher, I., C.C. & Aubry, M.-P.,
1995. A revised Cenozoic geochronology and chronostratigraphy.
In: W.A. Berggren, D.V. Kent, M.-P. Aubry and J. Hardenbol
(Editors), Geochronology, time scales and global stratigraphic
correlation. Special Publication 54. Society of Economic
Paleontologists and Mineralogists (Tulsa): 129-212.
Bohaty, S. & Zachos, J.C., 2003. Significant Southern Ocean warm-
ing event in the late middle Eocene. Geology 31(11): 1017-1020.
Brinkhuis, H. & Visscher, H., 1995. The upper boundary of the
Eocene series: a reappraisal based on dinoflagellate cyst
biostratigraphy and sequence stratigraphy. In: W.A. Berggren,
D.V. Kent, M.-P. Aubry & J. Hardenbol (eds), Geochronology,
time scales and global stratigraphic correlation. Special Publication
54. Society of Economic Paleontologists and Mineralogists
(Tulsa): 295-304.
Buchardt, B., 1978. Oxygen isotope palaeotemperatures from the
Tertiary period in the Norh Sea area. Nature 275: 121-123.
De Coninck, J., 2001. Organic-walled microfossils in the Oligocene
Grimmertingen and Neerrepen Sand Members from the
Grimmertingen type locality. Professional Paper 294(2): 1-57.
Dumont, A., 1849. Rapport sur la carte géologique de la Belgique.
Bulletin de l’Académie royale de Belgique, XVI(11): 351-373.
Lagrou, D., Vandenberghe, N., Van Simaeys, S. & Hus, J., 2004.
Magnetostratigraphy and rock magnetism of the Boom Clay
(Rupelian stratotype) in Belgium. Netherlands Journal of
Geosciences / Geologie en Mijnbouw 83(3): 209-225.
Lear, C.H., Elderfield, H. & Wilson, P., 2000. Cenozoic deep-sea
temperature and global ice volumes from Mg/Ca in benthic
foraminiferal calcite. Science 287: 269-272.
Miller, K.G., Feigenson, M.D., Wright, J.D. & Clement, B.M.,
1991. Miocene isotope reference section, Deep Sea Drilling
Project site 608: an evaluation of isotope and biostratigraphic
resolution. Paleoceanography 6(1): 33-52.
Miller, K.G. Mountain, G.S., Browning, J.V., Kominz, M.,
Sugarman, P.J., Christy-Blick, N., Katz, M.E. & Wright, J.D.,
1998. Cenozoic global sea level, sequences, and the New Jersey
transect: results from coastal plain and continental slope drilling.
Reviews of Geophysics 36(4): 569-601.
Odin, G.S. & Montanari, A., 1989. Age radiométrique et stratotype
de la limite Eocène Oligocène. Comptes Rendus de l’Académie
des Sciences de Paris, série II, 309: 1939-1945.
Schmitz, B., Heilmann-Clausen, C., King, C., Steurbaut, E.,
Andreasson, F.P., Corfield, R.M. & Cartlidge, J.E., 1996. Stable
isotope and biotic evolution in the North Sea during the early
Eocene; the Albaek Hoved section, Denmark. In: R.W.O.B.
Knox, R.M. Corfield and R.E. Dunay (eds), Correlation of the
early Paleogene in Northwest Europe. Geological Society of
London, Special Publication 101: 275-306.
Sissingh, W., 2003. Tertiary paleogeographic and tectonostrati-
graphic evolution of the Rhenish Triple Junction. Palaeogeo-
graphy, Palaeoclimatology, Palaeoecology 196: 229-263.
Steurbaut, E., 1992. Integrated stratigraphic analysis of lower
Rupelian deposits (Oligocene) in the Belgian Basin. Annales
Société Geologie Belgique 115(1): 287-306.
Stover, L.E. & Hardenbol, J., 1994. Dinoflagellates and depositional
sequences in the Lower Oligocene (Rupelian) Boom Clay
Formation, Belgium. Bulletin de la Société belge de Géologie
102(1-2): 5-77.
Thomas, E., Zachos, J.C. & Bralower, T.J., 2000. Deep-sea
environments on a warm earth: latest Paleocene-early Eocene.
In: B.T. Huber, K.G. Macleod & S.L. Wing (eds), Warm
Climates in Earth History. University Press, Cambridge UK
(Cambridge): 132-160.
Van Simaeys, S., De Man, E., Vandenberghe, N., Brinkhuis, H. &
Steurbaut, E., 2004. Stratigraphic and palaeoenvironmental
analysis of the Rupelian-Chattian transition in the type region:
evidence from dinoflagellate cysts, foraminifera and calcareous
nannofossils. Palaeogeography, Palaeoclimatology, Palaeoecology
208: 31-58.
Vandenberghe, N., Brinkhuis, H. & Steurbaut, E., 2003. The
Eocene/Oligocene boundary in the North Sea area: a sequence
stratigraphic approach. In: D.D. Prothero, L.C. Ivany & E.A.
Nesbitt (eds), From Greenhouse to Icehouse. The Marine
Eocene-Oligocene Transition. Columbia University Press (New
York): 419-437.
Vandenberghe, N., Hager, H.,Van Den Bosch, M.,Verstraelen, A.,
Leroi, S., Steurbaut, E., Prüfert, J. & Laga, P., 2001. Strati-
graphic correlation by calibrated well logs in the Rupel Group
between North Belgium, the Lower-Rhine area in Germany and
Southern Limburg and the Achterhoek in The Netherlands. In:
N. Vandenberghe (ed), Contributions to the Paleogene and
Neogene Stratigraphy of the North Sea Basin. Aardkundige
Mededelingen 11. Leuven University Press (Leuven): 69-84.
Vandenberghe, N., Laga, P., Steurbaut, E., Hardenbol, J. & Vail,
P.R., 1998. Tertiary sequence stratigraphy at the Southern
border of the North Sea basin in Belgium. In: P.-C. de
Graciansky, J. Hardenbol,T. Jacquin & P.R.Vail (eds), Mesozoic
and Cenozoic sequence stratigraphy of European Basins. SEPM
(Society for Sedimentary Geology), Tulsa, Oklahoma, U.S.A.:
119-153.
Winkelmolen, A.M., 1972. Shape sorting in Lower Oligocene,
Northern Belgium. Sedimentary Geology, 7: 183-227.
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, S., 1996. High-resolution
(104years) deep-sea foraminiferal stable isotope records of the
Eocene-Oligocene climate transition. Paleoceanography 11(3):
251-266.
Ziegler, P.A., 1990. Geological Atlas of Western and Central
Europe. 2nd edition. The Hague: Shell International Petroleum
Maatschappij B.V., 239 pp.


Stable oxygen isotope record of the Eocene-Oligocene transition in the southern North Sea Basin: positioning the Oi-1 event

Abstract

Similar works

Full text

Available Versions

Open Marine Archive