Cenomanian?Turonian carbonate platform deposits in west central Jordan

Schulze, Frauke; Lewy, Zeev; Kuss, Jochen; Gharaibeh, Ahmad

doi:10.1007/s00531-003-0339-6

Cited by 50 publications

(33 citation statements)

References 32 publications

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“…, 2001; Gertsch et al. , 2010) and Jordan (Schulze et al. , 2003, 2004, 2005) are marked by the presence of extensive oyster biostromes, which formed a specific facies in the Tethys and North Africa (Dhondt et al.…”

Section: Discussionmentioning

confidence: 99%

“…Oyster beds consist of 1 to 5 m thick biostromes and extend laterally over several hundreds of metres. Cenomanian strata of Morocco (Andreu, 1989), Sinai (Bauer et al, 2001;Gertsch et al, 2010) and Jordan (Schulze et al, 2003(Schulze et al, , 2004(Schulze et al, , 2005 are marked by the presence of extensive oyster biostromes, which formed a specific facies in the Tethys and North Africa (Dhondt et al, 1999).…”

Section: Sea-levelmentioning

confidence: 99%

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Middle and late Cenomanian oceanic anoxic events in shallow and deeper shelf environments of western Morocco

Gertsch¹,

Adatte

Keller³

et al. 2010

Sedimentology

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The response of shallow‐water sequences to oceanic anoxic event 2 and mid‐Cenomanian events 1a and 1b was investigated along the west African margin of Morocco north of Agadir (Azazoul) and correlated with the deep‐water sequence of the Tarfaya Basin (Mohammed Beach) based on biostratigraphy, mineralogy, phosphorus and stable isotopes. In the deeper Mohammed Beach section results show double peaks in δ13Corg for mid‐Cenomanian events 1a and 1b (Rotalipora reicheli biozone, lower CC10a biozone), the characteristic oceanic anoxic event 2 δ13C excursion (Rotalipora cushmani extinction, top of CC10a biozone) and laminated (anoxic) black shale. In the shallow environment north of Agadir, a fluctuating sea‐level associated with dysoxic, brackish and mesotrophic conditions prevailed during the middle to late Cenomanian, as indicated by oyster biostromes, nannofossils, planktonic and benthonic foraminiferal assemblages. Anoxic conditions characteristic of oceanic anoxic event 2 (for example, laminated black shales) did not reach into shallow‐water environments until the maximum transgression of the early Turonian. Climate conditions decoupled along the western margin of Morocco between mid‐Cenomanian event 1b and the Cenomanian–Turonian boundary, as also observed in eastern Tethys. North of Agadir alternating humid and dry seasonal conditions prevailed, whereas in the Tarfaya Basin the climate was dry and seasonal. This climatic decoupling can be attributed to variations in the Intertropical Convergence Zone and in the intensity of the north‐east trade winds in tropical areas.

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Section: Discussionmentioning

confidence: 99%

Section: Sea-levelmentioning

confidence: 99%

Middle and late Cenomanian oceanic anoxic events in shallow and deeper shelf environments of western Morocco

Gertsch¹,

Adatte

Keller³

et al. 2010

Sedimentology

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“…A key feature of the Whadi El Ghaib section is the presence of oyster-rich limestone beds during the late Cenomanian, as also observed in Morocco (Andreu 1989), in Sinai (Bauer et al 2003) and Jordan (Schulze et al 2003(Schulze et al , 2004(Schulze et al , 2005. During the Cretaceous, oysters typically inhabited shallow-water environments of the Tethys near North Africa where they first appeared during the late Aptian (Algeria and Morocco) and formed specific facies since the Cenomanian (Dhondt et al 1999).…”

Section: Micro-and Macrofossils As Environmental Proxiesmentioning

confidence: 99%

Cenomanian–Turonian transition in a shallow water sequence of the Sinai, Egypt

Gertsch

Keller

Adatte

et al. 2008

Int J Earth Sci (Geol Rundsch)

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Environmental and depositional changes across the Late Cenomanian oceanic anoxic event (OAE2) in the Sinai, Egypt, are examined based on biostratigraphy, mineralogy, d13 C values and phosphorus analyses. Comparison with the Pueblo, Colorado, stratotype section reveals the Whadi El Ghaib section as stratigraphically complete across the late Cenomanian-early Turonian. Foraminifera are dominated by high-stress planktic and benthic assemblages characterized by low diversity, lowoxygen and low-salinity tolerant species, which mark shallow-water oceanic dysoxic conditions during OAE2. Oyster biostromes suggest deposition occurred in less than 50 m depths in low-oxygen, brackish, and nutrient-rich waters. Their demise prior to the peak d 13 C excursion is likely due to a rising sea-level. Characteristic OAE2 anoxic conditions reached this coastal region only at the end of the d 13 C plateau in deeper waters near the end of the Cenomanian. Increased phosphorus accumulations before and after the d 13 C excursion suggest higher oxic conditions and increased detrital input. Bulk-rock and clay mineralogy indicate humid climate conditions, increased continental runoff and a rising sea up to the first d 13 C peak. Above this interval, a dryer and seasonally well-contrasted climate with intermittently dry conditions prevailed. These results reveal the globally synchronous d 13 C shift, but delayed effects of OAE2 dependent on water depth.

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“…The pattern boundary R3 is interpreted as the top of Paleozoic, the pattern boundary R4 as top of Precambrian. Khalil, 1993;Schulze et al, 2003) shows that these platform cover sequences are deformed into wide NNE-trending anticlines and synclines characteristic of the Santonian to Eocene Syrian Arc deformation episode. Thus, we suggest that the Al Kharrar monocline started to form at the early stages of the evolution of the Dead Sea Transform fault, overprinting older Syrian Arc structures.…”

Section: Discussionmentioning

confidence: 97%