An Early Cretaceous Volcanic Sequence in Central Israel and Its Significance to the Absolute Date of the Base of the Cretaceous

Lang, B.; Mimran, Y.

doi:10.1086/628939

Cited by 26 publications

(12 citation statements)

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“…The fossil‐bearing layer is a 2‐ to 3‐m thick layer of shales exposed in a small gully leading to Wadi el‐Malih, which flows from the Shomron to the Jordan Valley. This layer lies between a volcanic flow dated to 144–148 Ma and a flow dated to 122–134 Ma, placing it within the Hauterivian Period (Lang and Mimran 1985). These shales are composed of alternating layers of gypsum and clay and include many fossils of freshwater organisms.…”

Section: Introductionmentioning

confidence: 97%

“…Shomronella jordanica (Estes et al 1978) is found in a single location in the Tayasir Formation of the Shomron (Samaria) region of the West Bank. The Tayasir Formation is a 230‐m thick series of volcanics dated to the Lower Cretaceous (Lang and Mimran 1985). The fossil‐bearing layer is a 2‐ to 3‐m thick layer of shales exposed in a small gully leading to Wadi el‐Malih, which flows from the Shomron to the Jordan Valley.…”

Section: Introductionmentioning

confidence: 99%

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Ancient ontogenies: larval development of the Lower Cretaceous anuran Shomronella jordanica (Amphibia: Pipoidea)

Chipman

Tchernov

2002

Evolution and Development

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The Lower Cretaceous anuran Shomronella jordanica (Pipoidea) is represented by an assemblage of nearly 300 tadpoles of different ages. The size of the assemblage allows a reconstruction of the larval ontogeny of this species. We describe the ossification sequence and growth rates of S. jordanica and present reconstructions of tadpoles at different stages. The ontogeny of the species seems to be similar to that of extant pipids in many aspects. Larvae are similar in shape and size to those of Xenopus laevis but lack the anterior barbels that are typical for all extant pipids. The ossification sequence is closer to that of pipids than to that of other anurans. We present evidence that suggests that this species was terrestrial as an adult, and we discuss the implications of these data for the evolution of anuran development.

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Section: Introductionmentioning

confidence: 97%

Section: Introductionmentioning

confidence: 99%

Ancient ontogenies: larval development of the Lower Cretaceous anuran Shomronella jordanica (Amphibia: Pipoidea)

Chipman

Tchernov

2002

Evolution and Development

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“…West of the Dead Sea Rift in the Kurnub (Hathira) area (Figure 4), the unit ranges from Berriasian to Hauterivian at the base (Rosenfeld and Raab, 1984) and Barremian to Albian for the middle and upper part (Greenberg, 1968). Volcanic rocks intercalated in the basal Kurnub Sandstone, west of the Dead Sea Rift indicate a Berriasian to Valanginian age (Lang and Mimran, 1985).…”

Section: Kurnub Sandstone Groupmentioning

confidence: 98%

“…First, longerterm fluctuations in climatically driven eustatic sea level (Haq et al, 1988;Sharland et al, 2001); second, the configuration of the Neo-Tethys Ocean and its spreading centre near Cyprus; and third, the isostatic and intra-plate tectonic deformation of the Arabian Neoproterozoic Shield and its Palaeozoic sedimentary cover rocks, to the south and east, which influenced terrigenous siliciclastic sediment flux. Subsequent to Late Jurassic -Early Cretaceous extensional rifting (Bandel, 1981;Powell and Moh'd, 1993) and associated intra-plate continental volcanic activity (Lang and Mimran, 1985), the Early Cretaceous marks a period of post-rift flexural subsidence of the 'passive' continental margin. However, superimposed on this general trend were phases of local extensional tectonics (Barremian to Albian) in the Sinai (Bachmann et al, 2010), compressional/transpressional (Levant Plate/Syrian Arc) and extensional deformation (Arabian Plate), isostatic uplift, karstic erosion and gravitational slump-folding, in Late Cretaceous (Coniacian to Maastrichtian) times (Flexer et al, 1986;Cohen et al, 1990;Powell, 1989).…”

Section: Regional Geological Setting and Stratigraphymentioning

confidence: 99%

Evolution of Cretaceous to Eocene alluvial and carbonate platform sequences in central and south Jordan

Powell¹,

Moh’d²

2011

GeoArabia

130

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The Cretaceous to Eocene succession in central and south Jordan is characterised by passive continental margin depositional sequences, which pass upward from alluvial/paralic to carbonate shelf and pelagic ramp settings. Detailed section logging and outcrop mapping have produced robust lithostratigraphic and lithofacies schemes that can be correlated throughout the region and in the subsurface. These schemes are set in a sequence-stratigraphic context in relation to the evolution sedimentation on the Arabian and Levant plates. Three major megasequences are described (Kurnub, Ajlun and Belqa), and these are further subdivided into large-scale depositional sequences separated by regional sequence boundaries that represent maximum flooding surfaces. There is close correspondence between maximum flooding surfaces recording major sea-level rise with those derived for the Arabian and Levant plates, although there are some discrepancies with the precise timing of global sea-level fluctuations. An upward change from braided to meandering stream fluvial environments in central and south Jordan during the Early Cretaceous, reflects a decreasing geomorphological gradient of the alluvial plain, declining siliciclastic sediment flux, and increased floodplain accommodation, associated with a regional Late Albian (second-order) rise in relative sea-level. The Late Albian to Early Cenomanian marine transgression across the coastal alluvial plain marks a major sequence boundary. During Cenomanian to Turonian times a rimmed carbonate-shelf was established, characterised by skeletal carbonates showing small-scale, upward-shallowing cycles (fourth- to fifth-order parasequences) ranging from subtidal to intertidal facies, arranged into parasequence sets. Rimmed carbonate shelf sequences pass laterally to coeval coastal/alluvial plain facies to the south and east. Eustatic (third-order) fluctuations in relative sea level during the Cenomanian and Early Turonian resulted in deposition of ammonite-rich wackestones and organic-rich marls, during high sea-level stands (maximum flooding surfaces). Progradational sabkha/salina facies passing landwards to fluvial siliciclastics were deposited during an Early Turonian sea-level low stand, marks a regional sequence boundary, above which a highstand carbonate platform was established. A second-order, regional rise in sea level and marine transgression during the Early Coniacian marks a Type 2 sequence boundary, and subsequent drowning of the rimmed carbonate shelf by Late Coniacian times. Sedimentation during the Santonian to Maastrichtian was characterised by a hemi-pelagic chalk-chert-phosphorite lithofacies association, deposited in shallow to moderate water depths on a homoclinal ramp setting, although thicker coeval sequences were deposited in extensional rifts. The marked change in sedimentation from rimmed carbonate shelf to pelagic ramp is attributed to Neo-Tethyan mid-oceanic rifting, tilting, intracratonic deformation and subsidence of the platform; this is reflected in changes in biogenic productivity and ocean currents. Oceanic upwelling and high organic productivity resulted in the deposition of phosphorite together with giant oyster banks, the latter developing within oxygenated wave-base on the inner ramp. Chalk hardgrounds, sub-marine erosion surfaces, and gravitational slump folds indicate depositional hiatus and tectonic instability on the ramp. In the Early Maastrichtian, deeper-water chalk-marl, locally organic-rich, was deposited in density-stratified, anoxic basins, that were partly fault controlled. Pulsatory marine onlap (highstand sequences) during the Eocene is manifested in pelagic chalk and chert with a paucity of benthic macro-fauna, indicating a highly stressed, possibly hypersaline, and density-stratified water column. Comparison with global and regional relative sea-level curves enable regionally induced tectonic factors (hinterland uplift and ocean spreading) to be deduced, against a background of global sea-level rise, changing oceanic chemistry/productivity and climatic change.

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“…On the west side, the Tayasir Volcanics in Samaria (Mimran, 1972) underlie the clastic Hatira Formation. The volcanics were assigned to the lower part of the Neocomian with radiogenic ages of 138-133 Ma (Lang and Mimran, 1985). On the Manara slope exposure and the Hula 2 borehole, this section is about 600 m thick and the basalt flows, each a few tens of meters, are concentrated in three horizons in its middle part.…”

Section: Lower Cretaceous (Kurnub Group and Lower Parts Of Judea Group)mentioning

confidence: 99%

Geology of the Metulla quadrangle, northern Israel: Implications for the offset along the Dead Sea Rift

Sneh¹,

Weinberger²

2003

Israel Journal of Earth Sciences

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A stratigraphic analysis of Jurassic to Eocene rock units in the Metulla quadrangle provides ample evidence for a left-lateral offset based on the differences between the two sides of the Dead Sea Rift (DSR). The stratigraphic evidence for this offset is as follows: (1) The Jurassic Kidod shales of Mount Hermon face a limestone domain on the west side of the DSR throughout all of the Galilee; (2) the Neocomian volcanic sequence east of the DSR at the base of the Hatira sandstones in Mount Hermon is equivalent to the Tayasir Volcanics to its west in northern Samaria, and is different from the volcanic sequence of the Naftali Mountains and of Gebel Niha, which occur higher in the stratigraphic section; (3) sandstones of the Aptian Hidra Formation exposed in Mount Hermon are correlated with sandstones from the same stratigraphic unit in Samaria, while the Hidra Formation in the Naftali Mountains lacks sandstones; (4) the Albian Mas'ada Formation of Mount Hermon comprises limestone in the lower part and marl above it, while the equivalent Rama Formation in the Naftali Mountains is basically a marl sequence; (5) the Turonian Bina Formation exposed in the Shamir "windows" is divided into three units comparable to the Derorim, Shivta, and Nezer formations in the Gilboa Mountains, 90 km to the south and west of the DSR; (6) the Paleocene Taqiye marls in the Hula 3 borehole, north of Kefar Gil'adi and less than 2 km to the east of the Qiryat Shemona fault (and west of the Tel Hay fault) is about 360 m thick, which is comparable with the 370-m section exposed in Nahal Bezeq 100 km to the south, only several kilometers west of the western fault of the DSR. The Taqiye Formation of the Naftali Mountains is much thinner, and it appears in a marl and chert facies. Based on the last evidence, we suggest that the Qiryat Shemona fault forms the boundary between the African and Arabian plates in northern Israel.

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An Early Cretaceous Volcanic Sequence in Central Israel and Its Significance to the Absolute Date of the Base of the Cretaceous

Cited by 26 publications

References 1 publication

Ancient ontogenies: larval development of the Lower Cretaceous anuran Shomronella jordanica (Amphibia: Pipoidea)

Ancient ontogenies: larval development of the Lower Cretaceous anuran Shomronella jordanica (Amphibia: Pipoidea)

Evolution of Cretaceous to Eocene alluvial and carbonate platform sequences in central and south Jordan

Geology of the Metulla quadrangle, northern Israel: Implications for the offset along the Dead Sea Rift

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