Lithofacies evidence for the Cretaceous-Paleogene sedimentary history of Eratosthenes Seamount, Eastern Mediterranean, in its regional tectonic context (Sites 966 and 967)

Abstract

Drilling during Leg 160 penetrated an Early-Late Cretaceous and early Oligocene succession of carbonates in Hole 967E, beneath the lower northern slope of Eratosthenes Seamount. Middle Eocene pelagic carbonates were also recovered in Hole 966F, beneath the plateau area of the seamount. The base of the succession at Site 967 comprises shallow-water limestones, including coral and calcareous red algae, and occasional large foraminifers, that are interpreted as accumulations in a lagoonal setting within a carbonate platform. Neritic sedimentation ended in the upper Aptian (Lower Cretaceous) and was followed by an Upper Cretaceous pelagic carbonate succession that spans the interval from upper Cenomanian to Maastrichtian. Upper Cretaceous pelagic carbonates are locally organic rich and contain common replacement chert. In Hole 967E, Maastrichtian pelagic carbonates are unconformably overlain by lithologically similar chalks of early Oligocene age, with evidence of extensive reworking of older taxa. Minor tectonic instability is indicated by the presence of syndepositional neptunian dikes and fissures. In Hole 966F, middle Eocene pelagic chalks include reworked biota, chert, and organic-rich layers. The Eratosthenes Upper Cretaceous and Paleogene bathyal carbonates accumulated on a relatively level, submerged platform, isolated from terrigenous or gravity input. The transition from a shallow, carbonate platform to a bathyal setting (Turonian or earlier), took place before submergence of carbonate platforms in the Levant (in the Coniacian). Upper Cretaceous deposition on Eratosthenes is interpreted to have taken place seawards of a zone of high biogenic productivity that affected the Levant continental margin. Eratosthenes was also located well south of the zone of ophiolite genesis and tectonic displacement in the Upper Cretaceous. Overall, the Cretaceous and Paleogene carbonates of Eratosthenes are consistent with accumulation on an initially shallow, then submerged, carbonate platform isolated within a southern branch of the Neotethyan ocean, adjacent to the North African continental margin.

Tectonic and sedimentary response to subduction and incipient continental collision in southern Cyprus, easternmost Mediterranean region

“…The basin is inferred to extend offshore, as indicated by Sites 966 and 967 of the Ocean Drilling Program (Robertson 1998c). Two overall fault trends are recognized: (1) NW-SE to NNW-SSE faults and (2) NNE -SSW to north-south faults.…”

Environmental evolution and geological significance of the Miocene carbonates of the Eratosthenes Seamount (ODP Leg 160)

“…Above a fractured limestone unit, Cretaceous (Aptian or older) neritic limestone was recovered in ODP Hole 967E ( Fig. 3; Premoli-Silva et al, 1998;Robertson, 1998a). This shallow-water carbonate unit contains micritic intraclasts, pellets, benthic foraminifera, calcareous algae, molluscs, and other skeletal grains (Premoli-Silva et al, 1998;Robertson, 1998a).…”

“…3; Premoli-Silva et al, 1998;Robertson, 1998a). This shallow-water carbonate unit contains micritic intraclasts, pellets, benthic foraminifera, calcareous algae, molluscs, and other skeletal grains (Premoli-Silva et al, 1998;Robertson, 1998a). This assemblage formed within the photic zone and suggests a low energy environment, interpreted as a lagoon (Premoli-Silva et al, 1998;Robertson, 1998a).…”

Source rock characterization of mesozoic to cenozoic organic matter rich marls and shales of the Eratosthenes Seamount, Eastern Mediterranean Sea

“…Analysis of the drilled intervals from the ODP Leg 160 campaign constrains the interpretation of the depositional environments of the Upper Cretaceous and younger strata (Emeis et al, 1996;Premoli-Silva et al, 1998;Staerker, 1998). Shallow water carbonate deposition was interrupted during the Cenomanian/Turonian and younger Upper Cretaceous sediments were deposited in a hemipelagic to pelagic environment (Robertson, 1998c). Later, Miocene shallow water carbonate build-ups formed on the ESM.…”

“…During the Messinian Salinity Crisis (MSC) the sediments of the ESM were most likely exposed and affected by extensive meteoric water flushing, karstification, dolomitization, as well as erosion (Robertson, 1998b). Subsequent drowning of the ESM during the Pliocene to Quaternary enabled the deposition of pelagic carbonates and sapropels (Robertson, 1998c).…”