supplementary material cenomanian sequence stratigraphy … · 2008-12-02 · supplementary...
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SUPPLEMENTARY MATERIAL Cenomanian Sequence Stratigraphy and Sea Level Fluctuations in the Tarfaya Basin (SW-Morocco) Wolfgang Kuhnt1, Ann Holbourn1, Andy Gale2, El Hassane Chellai3, William J. Kennedy4
1Institute for Geosciences, Christian-Albrechts-University, 24118 Kiel, Germany 2Department of Earth and Environmental Sciences, University of Portsmouth, Portsmouth PO1 3QL, UK 3Department of Geology, Faculty of Sciences Semlalia, Cadi Ayyad University-Marrakech, PO Box 2390, Marrakech, Morocco 4University Museum of Natural History, Oxford OX1 3PW, UK GEOLOGICAL SETTTING
The Mohammed Plage (MPL) succession and Shell-ONAREP Exploration
Well (S13) are situated in the northern onshore part of the Tarfaya-Laayoune coastal
basin in SW-Morocco (Fig. 1, Suppl. Fig. 1). This basin is bounded to the south by
the West African craton, to the east by the Palaeozoic fold belt of the Mauretanides
and the Precambrian Requibat Massif and to the north by the Precambrian Anti Atlas
High (Choubert et al., 1966). Maximum sediment accumulation occurred during the
Mesozoic and Paleogene in the offshore part of the basin on the present-day shelf and
upper slope (von Rad and Einsele, 1980). During the Miocene, the uplift of the
volcanic province of the Canary Islands considerably affected sedimentation patterns
between the Canaries and the NW African coastline and shifted the depocenter
westwards into the abyssal part of the basin. More than 500 m of Upper Cretaceous
pelagic sediments, mainly consisting of calcareous nannoplankton, clay, dispersed
biogenic silica, planktonic foraminifers and marine organic matter were deposited in
the northern part of the Tarfaya Basin with a regional depocenter near the town of
DR2009051
Tarfaya. Sedimentation rates exceeded 10 cm/kyr during transgressive phases,
allowing for investigation of climatic events on a centennial resolution, which is
comparable to climate change studies in the Quaternary (Kuhnt et al., 2001; 2004;
Kolonic et al., 2005).
Previous investigations of lithofacies, organic matter, microfossil assemblages
and carbonate microfacies in the Tarfaya Basin allowed two distinct depositional
systems to be identified in the Albian and Cenomanian to Campanian. The Albian is
dominated by terrigenous silici- and bioclastic sedimentation with low organic matter
of mainly terrestrial origin. Clay mineral assemblages are characterized by abundant
illite and chlorite, eroded from crystalline rocks outcropping in the Anti-Atlas and
Mauretanides, and by reworked kaolinite indicating active erosion around the Tarfaya
Basin (El Albani et al., 1999a). The Cenomanian to Campanian interval is
characterized by pelagic marls and limestones containing abundant marine organic
matter (Kuhnt et al., 1990; Kolonic et al., 2005). Higher mean content of smectite in
clay mineral assemblages and abundant pelagic macro- and microfaunas reflect
higher relative sea level (El Albani et al., 1999a). These Cenomanian-Campanian
sediments appear to have been deposited during the development of an open shelf
coastal upwelling-system (Einsele and Wiedmann, 1982; Kolonic et al., 2005).
The MPL succession is situated along the coastal cliff between the river
mouths of Oued Chebeika and Oued Amma Fatma in the northern part of the basin
between the towns of TanTan and Tarfaya (Suppl. Fig. 1). The succession dips gently
to the SW, and its stratigraphic base is close to the mouth of the Oued Laaguig, while
the top is near the topographic reference point “21 m” approx. 10 km NE of the mouth
of Oued Amma Fatma. Lower Cretaceous sediments are outcropping at the base of the
cliff, and the Upper Cretaceous succession is overlain by Moghrabian (Plio-
Pleistocene) shallow marine, clastic sediments. The MPL succession was initially
sketched and dated with ammonites in the early seventies (Wiedmann et al., 1978;
Wiedmann and Kuhnt, 1996 and unpublished field sketches). However, no detailed
sedimentological and paleontological investigation was undertaken until the late
nineties, due to the violent, armed conflict raging in the Western Sahara region for
many years. Initial interpretation of a shore-face to outer shelf paleobathymetric
position were based on sedimentological criteria such as the occurrence of calcareous
tempestites, hummocky cross stratification and limestone channels (El Albani et al.,
1999b) and micropaleontological evidence from benthic foraminiferal assemblage
counts (Gebhardt et al., 2004).
Well S13 was drilled in the most distal part of the Tarfaya Basin, a few
kilometers east of the town of Tarfaya (Suppl. Fig. 1). This well is stratigraphically
the most complete oil shale exploration well in the basin, since it was drilled well
beyond the bitumen rich zone (“zone riche”) down into the lower Cenomanian (Leine,
1986). Organic-carbon rich sediments in S13 exhibit conspicuous cyclicity, mainly
expressed in fluctuations of the organic carbon and pelagic carbonate contents. Two
prominent low frequency cycles (lower Cenomanian to late Turonian and late
Turonian to middle Campanian) were recognized, which reflect the UZA 2 and UZA3
second order supercycles in the Haq et al. (1987; 1988) sea level chart. Maximum
organic carbon burial associated with benthos-free, laminated sediments, indicating
bottom water anoxia occurred during 3rd order sea level highstands in the latest
Cenomanian and early-middle Turonian. These intervals coincide approximately with
sea level highstands of the Haq et al. (1987; 1988) sea level chart.
Higher frequency variability in organic matter-carbonate percentages was
additionally detected with dominant periodicities around 100 and 40 kyr (Kuhnt et al.,
1997; 2004). These cycles, which are best expressed in the density logging data of
Shell-ONAREP exploration wells in the more distal part of the Tarfaya Basin, were
used as a powerful regional stratigraphic correlation tool. A total of 26 cycles was
discriminated, allowing detailed basinwide correlation of organic-rich sediments from
the upper part of the late Cenomanian Rotalipora cushmani Zone to the lower part of
the late Turonian Marginotruncana schneegansi Zone. The cyles were labelled cycles
-4 to -1 in the upper part of the R. cushmani Zone, cycle 0 including the extinction
level of R. cushmani, and cycles 1 to 22 in the Whiteinella archaeocretacea and
Helvetoglobotruncana helvetica Zones (Kuhnt et al., 1997; 2004). The logging record
ends in the uppermost part of the thick limestone-dominated interval between 201 and
208 m, which is correlative to the prominent limestone bed 1.26 in the MPL
succession.
BIOSTRATIGRAPHY
Mohammed Plage succession
The position of zonal boundaries for the R. brotzeni (= R. globotruncanoides),
R. reicheli, R. cushmani, and W. archaeocretacea Zones is based on the planktic
foraminiferal zonation of Caron (1985) and Robaszynski and Caron (1995), with
some modification, as the first appearance of R. reicheli appears to be latitudinally
diachronous (Robaszynski et al., 1994). While R. reicheli first appears in the upper
part of the Dixoni Zone in the late early Cenomanian of the Boreal realm, its first
occurrence is slightly later in the basal middle Cenomanian of the Tethyan realm
(Robaszynski et al., 1993). In the Tarfaya Basin, we place the lower/middle
Cenomanian boundary (corresponding to the Dixoni/Rhotomagense ammonite zonal
boundary) just below the first occurrence of R. reicheli, at an intermediate position
between the Boreal and Tethyan correlations. In contrast to Robaszynski and Caron
(1995), we also use the last occurrence of R. reicheli in the middle of the
Rhotomagense Zone as the top of the R. reicheli Zone, since the first occurrence of R.
cushmani is difficult to define because this species is scarce, and shows gradual
evolution from R. montsalvensis in the lower middle Cenomanian. Moreover, the
stratigraphic position of the first occurrence of R. cushmani in relation to the
ammonite zonation strongly differs in the Boreal and Tethyan realms, whereas the LO
of R. reicheli is approximately synchronous (Robaszynski and Caron, 1995). We
additionally note that the extinction of R. greenhornensis, which normally occurs ~30
kyr before the extinction of R. cushmani, is coeval with the extinction of R. cushmani
(top of the R. cushmani Zone corresponding to the upper part of the Geslinianum
ammonite Zone) at the base of Unit 4 (bed 4.94) in the MPL succession, thus
indicating the presence of a hiatus.
The planktonic foraminiferal biostratigraphy of the MPL succession is
corroborated by ammonite collections from individual beds. The lowest Cenomanian
fauna is found in the summit of bed 9.17, and includes elements typical of the lowest
Cenomanian Neostlingoceras carcitanense Subzone, such as Neostlingoceras sp. and
Utaturiceras bethlahemense. The presence of the overlying Sharpeiceras schluteri
Subzone (Gale, 1995) is reflected by the occurrence of Sharpeiceras sp. in bed 7.26.
The highest lower Cenomanian ammonites are found in bed 6.2, above which
ammonites are absent up until bed 3.2. The lowest middle Cenomanian fauna is found
in bed 3.2, including Cunningtoniceras cunningtoni, a species typical of the C. inerme
Zone (Gale, 1995). This zone extends up to bed 3.12. Acanthoceras sp. including A.
rhotomagense, reflect the presence of the A. rhotomagense Zone from bed 2.13 up to
bed 1.26. This fauna includes Calycoceras (Newboldoceras) cf. vergonense in bed
2.06, suggestive of the Turrilites acutus Subzone.
Shell-ONAREP Well S13
All four globally recognized Cenomanian planktonic foraminiferal zones were
identified in S13 (Kuhnt et al., 1990, Fig. 8):
(1) lower Cenomanian R. brotzeni – globotruncanoides Zone (358-278 m)
(2) latest lower to middle Cenomanian R. reicheli Zone (278-232 m)
(3) late Cenomanian R. cushmani Zone (232-183.2 m)
(4) latest Cenomanian W. archaeocretacea Zone (183.2-95 m), spanning the
Cenomanian/Turonian boundary
Within the expanded pelagic sequence in S13, several bio-events allow a
further subdivision of the four standard planktic foraminiferal zones. The last
occurrence (LO) of R. greenhornensis provides a distinct datum in the upper part of
the R. cushmani Zone, about 3.3 m below the final extinction of R. cushmani.
Immediately above the LO of R. greenhornensis a marked increase in radiolarian
abundance and the occurrence of ‘atypical’ specimens of R. cushmani with a high
trochospire and weakly developed keels were noted (Luderer and Kuhnt, 1997). This
change in zooplankton assemblage composition correlates with a pronounced positive
δ13C excursion in both carbonate and organic carbon (Kuhnt et al., 1990; Luderer and
Kuhnt, 1997). Above the extinction of R. cushmani s.l. at 183.2 m, planktonic
foraminiferal assemblages are dominated by hetereohelicids and unkeeled trochospiral
forms of Hedbergella and Whiteinella, including typical representatives of the zonal
marker W. archaeocretacea.
PALEOBATHYMETRY
Results from a canonical correspondence analysis (CCA), based on benthic
foraminiferal assemblage counts, P/B-ratio and planktic foraminiferal morphogroups
(Gebhardt et al., 2004) support the paleobathymetric assignment of sedimentary
sequences in the MPL succession. The most significant factor recognized in the
ordination of benthic species and samples was water depth. The CCA identified
Bolivina anambra, Globulina lacrima, Lenticulina spissocostata and
Spiroplectammina sp. as typical “shallow water species”, and Praebulimina nannina,
Gavelinella dakotensis, Gavelinella sp., Saccammina alexanderi and Valvulineria
lenticula as “deep water species”. The suite of benthic foraminiferal assemblages
points to repeated periods of shallowing within a general deepening trend in the lower
part of the succession (R. brotzeni and R. reicheli Zones). In contrast, assemblages
from the upper part of the succession (R. cushmani and W. archaeocretacea Zones)
do not contain any shallow water indicators.
According to Gebhardt et al. (2004), a first sea level rise occurred between
beds 7.1 and 7.25, followed by a sea level fall (beds 7.25-7.26). The next rise, which
began in beds 7.28-7.30, continued until bed 6.17. A minor regression in beds 5.1-5.2
was succeeded by a long transgressive phase, continuing until deposition of beds 3.2-
3.8. A prominent regressive episode, indicated by unsually low P/B-ratios and paralic
benthic foraminiferal assemblages, occurred during deposition of the dark greenish
gray claystone in bed 3.9. This major regression was followed by a further
transgression (beds 3.12-3.19). A brief sea level drop is indicated in bed 2.1 by low
P/B-ratios and CCA values. A less pronounced fall occurred at the end of the R.
reicheli Zone (bed 2.12) within the main transgressive trend. A minor regression is
further indicated in beds 4.37 to 4.40 by lower P/B-ratios and CCA values.
REFERENCES Caron, M., 1985, Cretaceous planktic foraminifera, in Bolli, H.M., Saunders, E., and Perch-Nielsen,
K., eds., Plankton stratigraphy, Cambridge, Cambridge University Press, p. 17-86. Choubert, G., Faure Muret, A., and Hottinger, L. 1966, Aperçu géologique du Bassin côtier de
Tarfaya (Stratigraphie), in Choubert, G., Faure Muret, A., Hottinger, L., Viotti, C., and Lecointre, G., eds., Le Bassin côtier de Tarfaya (Maroc Méridional): Notes et Mèmoires Service Géologique du Maroc, v. 175/1, p. 7-106.
Einsele, G., and Wiedmann, J. 1982, Turonian black shales in the Moroccan coastal basins: first upwelling in the Atlantic Ocean?, in von Rad, U., Hinz, K., Sarnthein, M., and E. Seibold, E., eds., Geology of the Northwest African Continental Margin: Berlin, Springer-Verlag, p. 393-414.
El Albani, A., Kuhnt, W., Luderer, F., Herbin, J.P., and Caron, M., 1999a, Paleoenvironmental evolution of the Late Cretaceous sequence in the Tarfaya Basin (southwest of Morocco), in Cameron, N.R., Bate, R.H., and Clure, V.S., eds., The Oil and Gas Habitats of the South Atlantic: Geological Society London, Special Publication, v. 153, p. 223-240.
El Albani, A., Vachard, D., Kuhnt, W., and Chellai, H., 1999b. Signature of hydrodynamic activity caused by rapid sea level changes in pelagic organic-rich sediments, Tarfaya basin (southern Morocco): C.R. Acad. Sci. Paris, Sciences de la terre et des planets, v. 329, p. 397-404.
Gale, A.S., 1995, Cyclostratigraphy and correlation of the Cenomanian Stage in Western Europe, in House, Mr.R., and Gale, A.S., eds., Orbital Forcing Timescales and Cyclostratigraphy: Geol. Soc. London Spec. Publ. v. 85, p. 177-197.
Gebhardt, H,, Kuhnt, W., and Holbourn, A., 2004, Foraminiferal response to sealevel change. Organic carbon flux and oxygen deficiency in the Cenomanian of the Tarfaya Basin, southern Morocco: Marine Micropaleontology, v. 53, p. 133-157.
Haq, B.U., Hardenbol, J., and Vail, P.R., 1987, Chronology of fluctuating sea levels since the Triassic: Science, v. 235, p. 1156-1167.
Haq, B.U., Hardenbol, J., and Vail, P.R., 1988, Mesozoic and Cenozoic chronostratigraphy and eustatic cycles, in Wilgus, C.K. et al., eds., Seal-level research: An integrated approach: Society of Economic Paleontologists and Mineralogists Special Publication,v. 42, p. 71-108.
Kolonic, S., Wagner, T., Forster, A., Sinninghe-Damsté, J.S., Walsworth-Bell, B., Erba, E., Turgeon, Brumsack, H.-J., Chellai, E.H., S., Tsikos, H., Kuhnt, W., and Kuypers, M.M.M., 2005, Mechanisms of black shale deposition at the NW-African Shelf during the Cenomanian/Turonian Oceanic Anoxic Event 2: implications for climate coupling and global organic carbon burial: Paleoceanography, v. 20, PA 1006, doi:10.1029/2003PA000950.
Kuhnt, W., Herbin, J. P., Thurow, J., and Wiedmann, J. 1990, Distribution of Cenomanian-Turonian organic facies in the western Mediterranean and along the adjacent Atlantic Margin, in Huc, A.Y., ed., Deposition of Organic Facies: AAPG Studies in Geology, v. 40, p. 133-160.
Kuhnt, W., Nederbragt, A., and Leine, L., 1997, Cyclicity of Cenomanian-Turonian organic-carbon-rich sediments in the Tarfaya Atlantic Coastal Basin (Morocco): Cretaceous Research, v. 18, p. 587-601.
Kuhnt, W., Chellai, E.H., Holbourn, A., Luderer, F., Thurow, J., Wagner, T., El Albani, A., Beckmann, B., Herbin, J.-P., Kawamura, H., Kolonic, S., Nederbragt, S., Street S., and Ravilious, K., 2001, Morocco basin’s sedimentary record may provide correlations for Cretaceous paleoceanographic events worldwide: EOS, Transactions, American Geophysical Union, v. 82/33, p. 361-364.
Kuhnt, W., Luderer, F., Nederbragt, S., Thurow, J., and Wagner, T., 2004, Orbital-scale record of the Late Cenomanian-Turonian Oceanic Anoxic Event (OAE-2) in the Tarfaya Basin (Morocco): International Journal of Earth Sciences, doi: 10.1007/s00531-004-0440-5.
Leine, L. 1986, Geology of the Tarfaya oil shale deposit, Morocco: Geologie en Mijnbouw, v. 65, p. 57-74.
Luderer, F., and Kuhnt, W., 1997, A high resolution record of the Rotalipora extinction in laminated organic-carbon rich limestones of the Tarfaya Atlantic coastal basin (Morocco): Ann. Soc. Geol. Nord, v. 5 (2éme série), p. 199-205.
Robaszynski, F., and Caron, M., 1995, Foraminifères planctoniques du Crétacé: commentaire de la zonation Europe-Méditerranée: Bull. Soc. Géol. France, v. 166, p. 681-692.
Robaszynski, F., Hardenbol, J., Caron, M., Amédro, F., Dupuis, C., González Donoso, J.-M., Linares, D., and Gartner, S., 1993, Sequence stratigraphy in a distal environment: the Cenomanian of the Kelaat Senan region of Central Tunisia: Bull. Centres Rech. Explor.-Prod. Elf Aquitaine, v. 17, p. 395-433.
Robaszynski, F., Caron, M., Amédro, F., Dupuis, C., Hardenbol, J., González Donoso, J.-M., Linares, D., and Gartner, S., 1994, Le Cénomanien de la region de Kelaat Senan (Tunisie centrale): litho-biostratigraphie et interpretation séquentielle: Revue de Paléobologie, Genève, v. 12, p. 351-505.
Von Rad, U., and Einsele, G., 1980, Mesozoic-Cainozoic subsidence history and palaeobathymetry of the northwest African continental margin (Aaiun Basin to D.S.D.P. Site 397): Philosophical Transactions of the Royal Society, London, A, v. 294,p. 37-50.
FIGURE CAPTIONS
Supplementary Figure 1: Topography and geology of MPL area with location of
logged sections along coastal cliff.
Supplementary Figure 2: Polished rock slabs showing characteristic lithologies in
S13: (1) organic carbon-lean, homogenous micritic limestones at 268.4 m; (2)
homogenous to strongly bioturbated marls with variable organic carbon content at
284.2 and 311.4 m; (3) organic-rich laminated marls at 177.0, 206.7, 216.1 and 277.7
m. Lower part of succession (lower to middle Cenomanian) is characterized by flame
structure bioturbation with rare intercalation of laminated TOC-rich intervals. Rare
limestone intervals exhibit irregular bedding structures probably representing
disconformities. Organic-rich laminated marls are more common in upper part of
succession, but bioturbation remains pervasive in early stage of OAE-2 carbon isotope
excursion (rock slab at 185.9 m).
Supplementary Figure 3: Selected thin sections of biomicritic limestones with
abundance of silt to fine sand size quartz grains estimated using particle analyzer tool
in ImageJ.
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n a e c O c i t n a l t A
Albian to lowermost CenomanianCenomanianUppermost Cenomanian-to Turonian
(Pliocene)Moghrebian
Pleistocene
Dunes
Perennial wetland
Perennial stream
Cliff
11°30´11°35´11°40´
11°45´
28°10´
28°15´
11°40´ 11°35´
28°15´
Topographical Base Map: Carte du Maroc- 1/200 000- Province de Tarfaya Feuille NG-28-XXIV (1963)
AA
B
AB Vertical exaggeration 1:2010 m30 m50 m
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Section 7Section 4 Se
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1Se
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2
Sect
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5Se
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Section 3
ATLANTIC OCEAN
0 2 4 6 8 km
72
38
8
“Mohammed Plage”
Mohammed Plage
11°45´
N
Supplementary Figure 1
Supplementary Figure 2
Supplementary Figure 3
Supplementary Tables 1-6
Table 1: Mohammed Plage section: bed thicknesses
Table 2: Mohammed Plage section: composition of acid residues
Table 3: Mohammed Plage section: Stable isotope data
Table 4: Mohammed Plage section: Plankton/benthos ratios and total organic carbon
Table 5: Well S13: Stable isotope data
Table 6: Well S13: Pyrolisis data
SUPPLEMENTARY TABLE 1 Section Bed-number Thickness (cm) Top of bed (m above base) 4 4.100 175 60.03 4.99 3 58.28 4.98 50 58.25 4.97 5 57.75 4.96 77 57.70 4.95 6 56.93 4.94 120 56.87 4.93 30 55.67 4.92 13 55.37 4.91 10 55.24 4.90 20 55.14 4.89 12 54.94 4.88 13 54.82 4.87 3 54.69 4.86 4 54.66 4.85 18 54.62 4.84 25 54.44 4.83 35 54.19 4.82 80 53.84 4.81 12 53.04 4.80 22 52.92 4.79 8 52.70 4.78 47 52.62 4.77 4 52.15 4.76 5 52.11 4.75 3 52.06 4.74 12 52.03 4.73 24 51.91 4.72 48 51.67 4.71 32 51.19 4.70 19 50.87 4.69 7 50.68 4.68 18 50.61 4.67 4 50.43 4.66 12 50.39 4.65 3 50.27 4.64 13 50.24 4.63 13 50.11 4.62 6 49.98 4.61 9 49.92 4.60 25 49.83 4.59 7 49.58 4.58 15 49.51 4.57 12 49.36 4.56 28 49.24 4.55 120 48.96 4.54 3 47.76 4.53 2 47.73 4.52 10 47.71 4.51 8 47.61 4.50 80 47.53 4.49 20 46.73 4.48 10 46.53 4.47 10 46.43 4.46 50 46.33 4.45 15 45.83 4.44 20 45.68
4.43 20 45.48 4.42 15 45.28 4.41 15 45.13 4.40 30 44.98 4.39 25 44.68 4.38 15 44.43 4.37 50 44.28 4.36 15 43.78 4.35 30 43.63 4.34 15 43.33 4.33 80 43.18 4.32 10 42.38 4.31 30 42.28 4.30 70 41.98 4.29 80 41.28 4.28 10 40.48 4.27 20 40.38 4.26 70 40.18 4.25 2 39.48 4.24 20 39.46 4.23 12 39.26 4.22 17 39.14 4.21 5 38.97 4.20 8 38.92 4.19 10 38.84 4.18 14 38.74 4.17 5 38.60 4.16 15 38.55 4.15 7 38.40 4.14 20 38.33 4.13 5 38.13 4.12 20 38.08 4.11 35 37.88 4.10 20 37.53 4.9 15 37.33 4.8 40 37.18 4.7 25 36.78 4.6 60 36.53 4.5 20 35.93 4.4 25 35.73 4.3 10 35.48 4.2 30 35.38 4.1 20 35.08 2 2.17 15 34.88 2.16 8 34.73 2.15 18 34.65 2.14 10 34.47 2.13 20 34.37 2.12 40 34.17 2.11 8 33.77 2.10 11 33.69 2.9 9 33.58 2.8 6 33.49 2.7 38 33.43 2.6 13 33.05 2.5 12 32.92 2.4 35 32.80 2.3 13 32.45 2.2 12 32.32 2.1 20 32.20
3 3.20 5 32.00 3.19 23 31.95 3.18 15 31.72 3.17 30 31.57 3.16 6 31.27 3.15 4 31.21 3.14 15 31.17 3.13 50 31.02 3.12 115 30.52 3.11 5 29.37 3.10 11 29.32 3.9 120 29.21 3.8 8 28.01 3.7 20 27.93 3.6 8 27.73 3.5 5 27.65 3.4 12 27.60 3.3 15 27.48 5 5.17=3.4 10 27.33 5.16=3.3 15 27.23 5.15=3.2 10 27.08 5.14=3.1 75 26.98 5.13 7 26.23 5.12 60 26.16 5.11 8 25.56 5.10 20 25.48 5.8 8 25.28 5.8 25 25.20 5.7 12 24.95 5.6 18 24.83 5.5 6 24.65 5.4 18 24.59 5.3 40 24.41 5.2 48 24.01 5.1 8 23.53 6 6.17=5.0 70 23.45 6.16 10 22.75 6.15 40 22.65 6.14 7 22.25 6.13 8 22.18 6.12 4 22.10 6.11 15 22.06 6.10 4 21.91 6.9 6 21.87 6.8 3 21.81 6.7 1 21.78 6.6 3 21.77 6.5 2 21.74 6.4 3 21.72 6.3 2 21.69 6.2 160 21.67 7 7.30 30 20.07 7.29 7 19.77 7.28 25 19.70 7.27 15 19.45 7.26 20 19.30 7.25 130 19.10 7.24 25 17.80 7.23 15 17.55 7.22 6 17.40
7.21 8 17.34 7.20 10 17.26 7.19 10 17.16 7.18 10 17.06 7.17 10 16.96 7.16 4 16.86 7.15 5 16.82 7.14 15 16.77 7.13 10 16.62 7.12 5 16.52 7.11 12 16.47 7.10 5 16.35 7.9 25 16.30 7.8 20 16.05 7.7 5 15.85 7.6 15 15.80 7.5 5 15.65 7.4 15 15.60 7.3 5 15.45 7.2 10 15.40 7.1 230 15.30 8+9 8.3=9.16 100 13.00 8.2=9.15 10 12.00 8.1=9.14 230 11.90 9.13 10 9.60 8.0=9.12 25 9.50 9.11 230 9.25 9.10 40 6.95 9.9 60 6.55 9.8 60 5.95 9.7 40 5.35 9.6 45 4.95 9.5 140 4.50 9.4 75 3.10 9.3 135 2.35 9.2 35 1.00 9.1 65 0.65
SUPPLEMENTARY TABLE 2 sample number
position in
section (m)
percent acid
residue
quartz (% of
residue)
Mica (% of
residue)
pyrite (% of
residue)
organic aggregates
(% of residue)
aggl. foraminifers
(% of residue)
biosiliceous material (% of residue)
dino-cysts
percent terrigenous
sand
1.03 35.43 0.88 70 a a 10 10 10 0.621.05 35.83 3.35 35 30 25 15 1.171.07 A 36.65 0.50 20 15 40 15 a 0.101.07 B 36.98 0.06 40 5 30 20 5 a 0.031.09 36.58 5.38 10 80 10 0.541.10 37.43 0.64 60 25 10 a 5 a 0.381.12 37.98 13.16 10 90 1.321.14 38.23 1.69 50 10 30 10 0.851.16 38.48 10.93 10 90 1.091.18 38.67 0.94 20 25 50 5 a 0.191.25 39.47 5.72 100 01.26 A 39.83 0.18 20 75 5 0.041.26 B 40.28 0.64 80 10 10 02.04 32.63 0.04 75 10 15 0.032.06 A 32.99 7.25 7 93 0.512.06 B 33.24 0.48 60 10 30 a a 0.292.08 33.46 1.24 80 5 5 10 0.992.10 33.64 1.36 85 10 5 1.152.13 34.27 1.11 90 10 1.002.14 A 34.42 1.39 95 a 5 1.322.14 B 34.56 6.36 98 2 6.232.16 34.69 13.74 10 90 1.372.18 A 34.93 1.54 30 40 a 30 0.462.18 B 35.03 0.66 60 a 20 20 a 0.403.02 27.03 3.54 98 1 1 a 3.473.04 27.28 0.84 65 a a 35 0.553.06 27.69 0.07 85 5 10 a 0.063.08 bottom
27.95 1.19 15 a a 80 5 0.18
3.08 top 27.97 0.07 70 a 25 5 0.053.09 B 28.16 0.35 40 40 5 15 0.143.09 D 28.31 0.19 30 65 a 5 03.09 F 28.46 0.23 a 100 03.09 H 28.61 0.17 100 03.09 L 28.76 1.46 90 10 0
3.09 N 28.91 1.41 100 03.09 P 29.06 0.00 a a 03.09 R 29.21 0.03 a 1 9 90 03.10 bottom
29.23 0.00 a 0
3.10 mid 29.26 0.24 100 03.10 top 29.29 0.00 45 30 35 99 03.12 A 29.53 3.56 70 a 30 a 2.493.12 B 29.69 0.07 85 a 3 6 6 a 0.063.12 C 29.85 3.05 10 70 20 a 0.303.12 D 30.01 0.48 50 a 40 a 10 a 0.243.12 E 30.17 0.32 75 a 5 10 5 5 0.243.12 F 30.33 0.21 35 a 5 30 10 20 0.073.12 G 30.49 0.37 80 a 5 5 a 10 a 0.303.14 31.10 0.50 90 4 2 4 a a 0.453.18 31.65 0.19 95 a a a 5 0.195.01 23.49 0.06 95 a 5 a a a 0.065.03 A 24.11 0.45 92 a 3 a 5 a 0.425.03 B 24.21 2.33 10 a 85 5 0.235.03 C 24.31 0.68 a a 100 a a 05.05 24.59 29.81 90 10 26.835.07 24.89 0.50 95 a 1 4 a a 0.475.09 25.24 0.13 40 a a 30 30 0.055.11 25.52 0.99 95 a 3 2 a 0.945.13 26.20 0.82 90 1 1 4 4 0.746.02 A 20.18 1.27 95 a 3 2 a 1.216.02 B 20.29 2.76 100 a a 0 a 2.766.02 C 20.40 1.94 100 a a 0 1.946.02 D 20.51 2.33 90 a 10 2.106.02 E 20.62 5.37 60 a a 40 3.226.02 F 20.73 5.81 100 a a a 5.816.02 G 20.84 6.88 100 a a a 6.886.02 H 20.95 3.43 80 2,5 2 15 2.756.02 I 21.06 2.40 97 3 a a 2.336.02 J 21.17 5.22 55 a 30 15 2.876.02 K 21.28 0.54 98 a a 2 a a 0.536.02 L 21.39 4.43 30 60 10 1.336.02 M 21.50 3.39 40 50 10 a 1.366.02 top 21.61 0.51 90 5 5 0.466.04 21.71 0.29 80 10 10 a a 0.236.06 21.76 0.31 75 15 10 a a 0.23
6.08 21.80 0.06 65 5 30 a a 0.046.10 21.89 0.11 20 a a 80 a a 0.026.11 21.99 0.23 a a 100 06.12 22.08 0.00 a 0 a 06.14 22.22 0.10 a 0 a 06.16 22.70 0.00 a 0 a 06.18 23.49 0.28 a a a 100 a a 07.01 top 14.15 0.43 100 a a a a 0.437.02 15.35 0.29 100 a a a 0.297.03 15.43 0.58 100 a a a 0.587.04 15.53 0.39 100 a a a 0.397.05 15.63 0.00 60 a a 40 a 07.06 15.73 1.04 83 10 7 a 0.867.07 15.83 1.75 50 a 50 a a 0.887.08 15.95 0.97 100 a a a 0.977.09 A 16.13 1.13 100 a a a a a 1.137.09 B 16.21 0.94 100 a a a a 0.947.11 16.41 1.44 90 a a 10 a 1.297.13 16.57 3.89 95 5 a a 3.697.15 16.80 1.81 80 a 15 5 1.447.17 16.91 0.71 75 a 5 20 a 0.537.19 17.11 0.50 40 5 50 5 0.207.21 17.30 0.24 30 30 40 a a 0.077.23 17.48 0.10 90 a 10 a a 0.097.25 A 17.93 0.63 35 a 5 60 a a 0.227.25 B 18.06 0.54 75 2 3 15 5 a 0.407.25 C 18.19 0.11 100 a a a a 0.117.25 D 18.32 1.12 60 3 35 2 0.677.25 E 18.45 0.47 60 a a 40 a 0.287.25 F 18.58 0.68 75 a a 20 5 0.517.25 G 18.71 0.96 75 2 5 13 5 0.727.25 H 18.84 0.73 95 a 5 a a 0.707.25 I 18.97 0.87 100 a a 0.877.27 19.38 1.49 100 a a 1.497.28 19.58 0.32 100 a a a a 0.327.29 19.74 3.89 20 5 75 a 0.78
a = accessory (<1%)
SUPPLEMENTARY TABLE 3 bed number depth (m) d13C d18O
7.1top 14.15 -0.44 -3.68
7.2 15.35 -0.41 -2.43 7.3 15.43 -0.40 -2.06 7.4 15.53 -0.25 -2.99 7.5 15.63 -0.39 -1.94 7.6 15.73 -0.86 -3.51 7.7 15.83 -1.17 -4.83 7.8 15.95 -0.81 -2.45
7.9A 16.13 -0.25 -1.56 7.9B 16.21 -0.41 -1.43 7.11 16.41 -0.54 -1.40 7.13 16.57 -0.85 -3.11 7.15 16.80 -0.67 -1.70 7.17 16.91 -1.21 -1.90 7.19 17.11 -0.87 -1.71 7.21 17.30 -0.60 -1.50 7.23 17.48 -0.53 -1.50
7.25A 17.93 -0.69 -1.27 7.25B 18.06 -0.43 -1.27 7.25C 18.19 -0.89 -1.43 7.25D 18.32 -0.76 -1.54 7.25E 18.45 -0.93 -1.80 7.25F 18.58 -0.73 -1.40 7.25G 18.71 -0.71 -1.51 7.25H 18.84 -0.47 -1.25 7.25I 18.97 -1.30 -2.13 7.27 19.38 -0.90 -1.56 7.28 19.58 -0.50 -1.12 7.29 19.74 -1.06 -1.68 6.2A 20.18 -1.34 -1.62 6.2B 20.29 -0.89 -1.45 6.2B 20.29 -1.00 -1.49 6.2C 20.40 -1.05 -1.88 6.2D 20.51 -0.82 -1.38 6.2E 20.62 -0.87 -1.32 6.2F 20.73 -1.12 -1.68 6.2G 20.84 -1.16 -2.40 6.2H 20.95 -0.77 -1.40 6.2I 21.06 -1.34 -1.86 6.2J 21.17 -1.03 -1.83 6.2K 21.28 -1.05 -1.89 6.2L 21.39 -1.06 -1.33 6.2M 21.50 -1.56 -1.59
6.2TOP 21.61 -1.31 -1.23 6.2TOP 21.61 -1.39 -1.25
6.4 21.71 -1.88 -1.66 6.6 21.76 -1.97 -2.42 6.8 21.80 -1.86 -2.03
6.10 21.89 -2.00 -1.57 6.11 21.99 -1.94 -1.50 6.12 22.08 -2.63 -2.19 6.14 22.22 -1.68 -1.38 6.16 22.70 -1.83 -1.36
5.1 23.49 -1.63 -1.22 6.18 23.49 -1.71 -1.12 5.3A 24.11 -1.46 -1.06 5.3B 24.21 -2.19 -1.42
5.3C 24.31 -3.34 -1.92 5.5 24.59 -2.22 -1.90 5.7 24.89 -1.56 -1.06 5.9 25.24 -1.61 -1.38
5.11 25.52 -1.80 -1.43 5.13 26.20 -0.51 0.42
3.2 27.03 -2.41 -2.44 3.2 27.03 -2.45 -2.22 3.4 27.28 -1.61 -1.33 3.6 27.69 -1.33 -1.16
3.8BOTTOM 27.95 -1.15 -1.68 3.8TOP 27.97 -1.09 -2.09
3.9B 28.16 -1.46 -1.62 3.9D 28.31 -1.40 -1.46 3.9F 28.46 -1.00 -1.26 3.9H 28.61 -0.76 -1.36 3.9L 28.76 -0.37 -1.54 3.9N 28.91 -0.52 -1.59 3.9P 29.06 -0.87 -1.50 3.9R 29.21 -0.96 -1.27
3.10BOTTOM 29.23 -1.04 -1.11 3.10BOTTOM 29.23 -1.07 -1.18
3.10MID 29.26 -0.87 -1.05 3.10TOP 29.29 -0.90 -0.96
3.12A 29.53 -2.48 -2.12 3.12B 29.69 -1.15 -1.25 3.12C 29.85 -1.15 -1.47 3.12C 29.85 -1.20 -1.63 3.12D 30.01 -1.22 -1.43 3.12E 30.17 -1.20 -1.38 3.12F 30.33 -1.04 -1.23 3.12G 30.49 -1.38 -1.27
3.14 31.10 -1.34 -1.64 3.18 31.65 -1.22 -1.34
2.4 32.63 -1.36 -1.30 2.6A 32.99 -1.00 -2.35 2.6A 32.99 -1.06 -2.43 2.6B 33.24 -1.31 -1.26
2.8 33.46 -1.00 -2.28 2.10 33.64 -1.45 -1.58 2.13 34.27 -1.27 -1.34
2.14A 34.42 -1.65 -2.11 2.14A 34.42 -1.84 -2.34 2.14B 34.56 0.45 -3.45
2.16 34.69 -1.66 -1.91 2.18A 34.93 -1.67 -1.62 2.18B 35.03 -1.03 -1.73
1.3 35.43 -2.08 -1.69 1.5 35.83 -2.65 -3.02
1.7A 36.58 -2.18 -1.77 1.7B 36.68 -2.15 -1.59
1.9 37.25 -0.30 -4.81 1.10 37.43 -3.20 -2.45 1.12 37.98 -0.76 -5.22 1.14 38.23 -3.27 -2.95 1.16 38.48 -0.30 -4.36 1.18 38.67 -2.58 -2.74 1.18 38.67 -2.57 -2.80 1.25 39.47 -0.16 -4.01
1.26A 39.83 -1.07 -2.98
1.26B 40.28 -2.81 -2.12 4.27 40.60 -0.11 -4.13 4.28 40.90 -0.61 -3.59 4.29 41.25 -0.18 -3.69 4.30 41.55 -2.32 -2.45
4.33_BASE 42.53 -2.21 -3.39 4.33_MID 42.90 -1.57 -3.33 4.33_TOP 43.25 -0.63 -3.65
4.35 43.55 -1.46 -3.48 4.37_BASE 44.03 -0.44 -2.58
4.37_TOP 44.45 -0.69 -3.74 4.39 44.70 -2.91 -3.58
4.40_BASE 44.80 -2.50 -2.82 4.43 45.50 -0.56 -3.22 4.45 45.73 -1.35 -3.46
4.46_BASE 45.80 -1.14 -3.25 4.46_TOP 46.47 -1.00 -3.25
4.48 46.62 -1.73 -3.08 4.50_75 46.70 -1.16 -3.00
4.51_BASE 46.87 -1.38 -2.94 4.51_TOP 47.45 -1.20 -3.11
4.55_1 48.00 -1.82 -2.86 4.55_35 48.65 -1.44 -3.07
4.57_BASE 49.39 -0.75 -3.26 4.61 49.95 -0.78 -3.85 4.62 50.05 -0.98 -4.12 4.64 50.27 -0.83 -2.66 4.70 50.90 -1.18 -3.04
4.72_40 51.30 -1.02 -2.58 4.72_20 51.50 0.58 -2.70 4.72_5 51.70 0.12 -2.97
4.74 52.09 -0.56 -2.82 4.78_42 52.25 -0.56 -2.93 4.78_20 52.47 -1.33 -3.28 4.78_5 52.62 0.86 -2.87
4.80 52.90 -0.50 -2.86 4.82_25 53.30 -0.48 -3.39 4.82_5 53.50 -0.93 -3.50
4.84_BASE 54.18 -0.75 -3.27 4.84_TOP 54.43 -0.82 -3.27
4.89 54.88 0.20 -3.02 4.94_145 55.70 0.90 -3.92 4.94_125 55.90 0.86 -3.93
4.94_95 56.20 -0.54 -4.20 4.94_65 56.50 0.53 -4.93 4.94_45 56.70 0.99 -3.54 4.94_35 56.80 0.44 -4.67 4.94_5 57.10 -3.50 -5.90
4.96_75 57.25 0.13 -3.58 4.96_5 57.95 0.67 -4.01
4.98_50 58.05 0.82 -3.94 4.98_25 58.30 0.73 -3.87 4.98_5 58.50 1.11 -4.17
4.100_170 58.65 1.57 -3.85 4.100_150 58.85 0.81 -4.08 4.100_120 59.15 1.54 -3.72
4.100_90 59.45 1.69 -3.76 4.100_60 59.75 1.12 -3.06 4.100_30 60.05 1.61 -3.38
4.100_0 60.35 0.82 -2.97
SUPPLEMENTARY TABLE 4 depth P/B-ratio TOC (%) 60.35 97 3.0 60.05 96 1.9 59.75 92 3.3 59.45 98 6.0 59.15 98 7.5 58.85 99 6.8 58.65 97 8.4 58.30 97 7.0 57.55 98 2.8 57.15 91 2.4 56.80 98 7.9 55.90 91 6.3 55.50 66 4.6 55.20 67 4.8 55.05 82 5.1 54.75 94 6.5 54.67 82 3.6 54.64 48 5.1 54.55 73 3.7 54.30 83 5.9 53.90 93 7.5 53.60 96 6.3 53.25 99 6.2 52.95 94 7.4 52.75 92 7.1 52.65 88 5.3 52.18 85 6.2 51.75 87 1.1 51.45 93 5.4 51.05 95 3.1 50.65 94 9.1 50.52 91 4.1 50.40 90 6.1 49.80 49 5.8 49.65 68 4.4 49.50 85 4.6 49. 11 6.0 48.25 81 6.7 47.90 67 5.9 47.75 60 5.0 46.20 96 8.7 45.65 88 4.7 45.30 57 5.2 45. 66 4.7 44.30 92 5.0 43.25 98 6.2 42.15 92 5.5 39.69 90 4.3 39.55 78 0.7 39.40 93 3.2 39.14 83 4.6 38.95 97 3.4 38.86 92 2.2
38.70 77 0.9 38.59 83 3.5 38.33 91 1.7 38.05 95 2.2 37.90 95 1.0 37.55 86 3.9 36.95 96 4.3 36.45 25 4.3 36.32 88 1.5 36.10 86 3.6 35.92 90 0.9 35.70 93 2.3 35.18 92 3.5 34.98 95 2.1 34.51 92 2.4 34.26 96 2.8 34.14 86 1.9 33.94 82 2.2 33.86 82 3.9 33.62 69 2.6 33.38 91 2.9 33.28 92 2.3 32.78 95 1.9 32.44 19 1.9 32.28 88 3.7 32.13 94 2.0 31.76 40 2.6 31.10 81 1.3 30.80 87 0.8 30.60 76 1.0 30.35 78 3.3 29.91 80 0.7 29.90 86 0.7 29.74 69 1.0 28.99 29 0.7 28.94 42 0.1 28.70 45 1.4 28.49 78 1.2 28.16 84 4.9 28.02 86 4.4 27.81 55 5.3 27.24 79 0.6 27.20 74 2.4 26.48 70 2.4 26.03 87 4.5 25.80 85 6.0 25.65 81 1.7 25.53 51 0.8 25.38 88 2.9 25.13 68 5.3 24.93 81 4.8 24.41 82 5.7 23.59 75 2.5 23.28 85 2.4 22.99 80 1.0 22.45 76 4.6
20.51 77 1.4 20.12 70 2.5 19.78 98 3.3 18.24 15 5.0 17.26 54 2.3 17.12 43 0.9 16.17 47 15.97 31 3.2 15.90 37 10.68 0 0.2 3.850 0 0.2
SUPPLEMENTARY TABLE 5 S13 depth d13Ccarb d13Corg
170.00 1.54 -25.00170.00 2.82 -25.06170.50 0.53 -25.02172.00 0.16 -24.60176.00 0.44 -24.50176.00 0.57 -25.69177.00 -1.21 -25.32178.00 1.50 -24.02179.00 2.35 -25.80181.70 3.63 -25.49182.00 2.18 -24.90182.00 2.64 -23.82182.20 3.01 -23.49182.60 1.72 -25.25183.20 2.77 -25.60183.70 2.62 -25.44184.10 2.66 -25.67185.00 1.58 -24.80185.30 2.04 -26.09186.20 0.79 -25.91186.80 0.25 -26.20187.00 2.27 -25.54188.00 3.15 -27.45188.50 1.27 -27.67188.90 1.01 -26.80189.40 0.45 -27.66190.00 0.46 -27.63190.30 0.06 -27.50190.90 -0.10 -27.60191.30 0.98 -27.44192.20 -0.81 -28.50192.20 -0.14 -27.70194.50 0.91 -27.11196.10 0.84196.10 0.90 -27.50197.50 -0.52 -28.13198.70 -2.34 -27.61199.20 1.51 -28.39200.40 -0.37201.00 0.44201.90 0.05201.90 -0.04 -28.24202.70 1.05205.70 0.58206.70 -1.15206.70 -0.28206.70 -0.30208.10 0.14208.90 -0.58209.70 -0.79210.60 0.52210.60 1.08212.30 -9.50213.40 -0.23213.40 0.38 -27.96213.40 -0.20214.10 0.39
216.10 0.33217.70 0.09219.50 -2.00223.00 -2.33223.20 -3.04225.00 -0.18225.90 -0.61228.80 0.00228.80 0.00232.50 -0.18236.00 0.75236.70 0.13239.50 0.62247.00 0.75247.00 0.64251.30 0.37251.80 -0.24254.00 0.19257.00 -0.70257.80 -0.13261.90 -0.36262.70 0.97262.70 1.02264.20 -0.27267.70 -2.45268.40 -0.92269.90 -0.87270.50 0.15 -27.88270.50 0.24277.70 -1.25277.70 -1.16279.50 0.28288.80 0.18289.30 -0.46296.30 -0.81297.20 -0.34298.50 -0.15302.50 -1.65307.30 -0.73311.00 -0.68311.40 -0.57311.40 -0.64314.00 -0.75314.10 -0.73319.40 -0.08322.00 -2.20323.30 -0.48328.40 -0.51331.00 -0.75331.00 -0.77334.00 -1.34336.00 -2.36342.60 -0.28347.00 -0.09349.10 0.22352.60 -0.85356.10 -0.57356.10 -0.61358.50 -0.48
SUPPLEMENTARY TABLE 6 sample #
thickness of sample (m)
depth middle (m)
oil (l/t) Fischer essai
OM (%)
69 2.00 170.00 65 7.3070 2.00 172.00 115 15.8071 2.00 174.00 98 14.4072 2.00 176.00 62 9.1073 2.00 178.00 98 15.2074 2.00 180.00 88 13.0075 2.00 182.00 48 7.6676 2.00 184.00 73 10.3077 2.00 186.00 63 9.6078 2.00 188.00 29 4.2079 2.00 190.00 80 12.4080 2.00 192.00 45 6.9081 2.00 194.00 49 7.2082 2.00 196.00 48 7.9083 2.00 198.00 43 8.3084 2.00 200.00 43 6.3085 2.00 202.00 43 6.2086 2.00 204.00 36 4.2087 2.00 206.00 35 5.0488 2.00 208.00 43 7.1089 3.00 210.50 32 6.0090 3.00 213.50 38 6.1091 3.00 216.50 36 5.9092 3.00 219.50 43 6.6093 3.00 222.50 38 5.8094 3.00 225.50 41 5.2095 3.00 228.50 36 5.4096 3.00 231.50 34 6.2097 3.00 234.50 32 4.2098 3.50 237.75 35 6.5099 5.50 242.25 29 4.90100 3.00 246.50 27 4.60101 3.00 249.50 37 6.40102 4.00 253.00 34 5.90103 4.00 257.00 32 6.30104 4.50 261.25 25 5.70105 4.00 265.25 25 5.70106 1.90 269.50 35 7.50107 4.15 273.00 23 5.70108 5.00 277.50 31 5.40109 5.00 282.50 18 6.60110 5.00 287.50 26 6.30111 5.00 292.50 20 6.20112 4.00 297.00 18 3.30113 4.00 301.00 17 5.90114 4.00 305.00 20 5.20115 4.00 309.00 15 5.00116 4.00 313.00 50 3.95117 4.00 317.00 50 3.75118 4.00 321.00 90 3.75119 4.00 325.00 50 4.30120 3.00 338.50 12 3.56121 2.00 351.00 11 4.50122 2.50 358.00 80 3.30