Late Palaeozoic sequence correlations, North Greenland, Svalbard and the Barents Shelf

Stemmerik, Lars; Worsley, David

doi:10.1007/978-94-009-1149-9_10

Cited by 48 publications

(53 citation statements)

References 20 publications

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“…The two fault zones in North Greenland are dominated by orthogonal N-S compression. The Kap Cannon Thrust Zone carries kilometres-thick metasedimentary rocks northwards on top of sedimentary rocks of the Wandel Sea Basin [12,23,61] and the volcanosedimentary units of the Upper Cretaceous Kap Washington Group [5,6,18,37,54,57]. The northwards increase in metamorphism in North Greenland mentioned above is probably related to thrusting of deep-seated Ellesmerian units upwards during the Eurekan deformation.…”

Section: Eurekan Deformationmentioning

confidence: 99%

Tectonic map of the Ellesmerian and Eurekan deformation belts on Svalbard, North Greenland, and the Queen Elizabeth Islands (Canadian Arctic)

Piepjohn

Gosen

Tessensohn³

et al. 2015

Arktos

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Section: Eurekan Deformationmentioning

confidence: 99%

Tectonic map of the Ellesmerian and Eurekan deformation belts on Svalbard, North Greenland, and the Queen Elizabeth Islands (Canadian Arctic)

Piepjohn

Gosen

Tessensohn³

et al. 2015

Arktos

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“…Sverdrup Basin, northern margin chloroforam, Nansen, Raanes bryonoderm, Great Bear Cape bryonoderm, Degerbols bryonoderm hyalosponge, unnamed unit Thorsteinsson, 1974;Davies and Nassichuk, 1991;Beauchamp, 1993Beauchamp, , 1994Beauchamp et al, 1995a,b;Beauchamp and Henderson, 1994;Beauchamp and Desrochers, 1997 9. North Greenland Gruszczynski et al, 1989;Stemmerik and Worsley, 1989;Ezaki et al, 1994;Stemmerik, 1997Stemmerik, , 2000 11. BjÖrnÖya Kiersnowski et al, 1995;Smith, 1981a,b cold water during the Guadalupian (Beauchamp, 1994;Beauchamp and Desrochers, 1997).…”

Section: Expansion Of Pce: Guadalupianmentioning

confidence: 99%

“…Among those are the Rex Chert and Tosi Chert members of the Phosphoria Formation in the western USA (Wardlaw and Collinson, 1986), which inter¢nger with fossiliferous, cold-water, bryonoderm carbonates with echinoderms, bryozoans, brachiopods and sponge spicules as the only constituents (Wardlaw and Collinson, 1986). Similar and coeval units include the chert-bearing Fantasque Formation of western Canada (Henderson et al, 1993), and Kapp Starostin Formation of Svalbard (Stemmerik and Worsley, 1989) and equivalent units in the Barents Sea (Stemmerik and Worsley, 1995).…”

Section: Expansion Of Pce: Guadalupianmentioning

confidence: 99%

“…As in the Sverdrup Basin, the Late Permian of the Svalbard^Barents Sea area has traditionally been interpreted as missing beneath a widespread sub-Triassic unconformity (see Stemmerik and Worsley, 1989). However, physical and geochemical evidence of Lopingian sedimentation and continuous deposition across the Permian^Triassic boundary has been documented in Svalbard (Gruszczynski et al, 1989;Wignall et al, 1998).…”

Section: Zenith Of Pce: Lopingianmentioning

confidence: 99%

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Growth and demise of Permian biogenic chert along northwest Pangea: evidence for end-Permian collapse of thermohaline circulation

Beauchamp

Baud

2002

Palaeogeography, Palaeoclimatology, Palaeoecology

269

132

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The Permian Chert Event (PCE) was a 30 Ma long episode of unusual chert accumulation along the northwest margin of Pangea, and possibly worldwide. The onset of the PCE occurred at about the Sakmarian^Artinskian boundary in the Sverdrup Basin, Canadian Arctic, where it coincides with a maximum flooding event, the ending of high-frequency/high-amplitude shelf cyclicity, the onset of massive biogenic chert deposition in deep-water distal areas, and a long-term shift from warm-to cool-water carbonate sedimentation in shallow-water proximal areas. A similar and coeval shift is observed from the Barents Sea to the northwestern USA. A landward and southward expansion of silica factories occurred during the Middle and Late Permian at which time warm-water carbonate producers disappeared completely from the northwest margin of Pangea. Biotically impoverished and increasingly narrow cold-water carbonate factories (characterised by non-cemented bioclasts of sponges, bryozoans, echinoderms and brachiopods) were then progressively replaced by silica factories. By Late Permian time, little carbonate sediments accumulated in the Barents Sea and in the Sverdrup Basin, where the deep-to shallow-water sedimentary spectrum was occupied by siliceous sponge spicules. By that time, biogenic silica sedimentation was common throughout the world. Silica factories collapsed in the Late Permian, abruptly bringing the PCE to an end. In northwest Pangea, the end-Permian collapse of the PCE was associated with a major transgression and with a return to much warmer oceanic and continental climatic conditions. Chert deposition resumed in the distal oceanic areas during the early Middle Triassic (Anisian) after a 8^10 Ma interruption (Early Triassic Chert Gap). The conditions necessary for the onset, expansion and zenith of the PCE were provided by the thermohaline circulation of nutrient-rich cold waters along the northwestern and western margin of Pangea, and possibly throughout the world oceans. These conditions provided an efficient transportation mechanism that constantly replenished the supply of silica in the area, created a nutrient-and oxygen-rich environment favouring siliceous biogenic productivity, established cold sea-floor conditions, hindering silica dissolution, while increasing calcium carbonate solubility, and provided conditions adverse to organic and inorganic carbonate production. The northwest margin of Pangea was, for nearly 30 Ma, bathed by cold waters presumably derived from the seasonal melting of northern sea ice, the assumed engine for thermohaline circulation.This process started near the Sakmarian^Artinskian boundary, intensified throughout Middle and Late Permian time and ceased suddenly in latest Permian time. It led to oceanic conditions much colder than normally expected from the palaeolatitudes, and the influence of cold northerly-derived water was felt as far south southern Nevada. The demise of silica factories was caused by the rapid breakdown of these conditions and the establishment of a much warm...

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“…No evidence of subaerial exposure or a hiatus has been recorded in central Spitsbergen (Mangerud & Konieczny, 1993). However, whether or not the Permo-Triassic boundary represents a period of Dallmann et al, 1999 erosion, non-deposition or conformable sedimentation remains controversial (Mørk et al, 1989;Stemmerik & Worsley, 1989;Mangerud & Konieczny, 1993;Ehrenberg et al, 2001;Nakrem et al, 2008;Dustira et al, 2013).…”

Section: Study Intervalmentioning

confidence: 99%

Facies arrangement and cyclostratigraphic architecture of the Templet Member and the Kapp Starostin Formation (Permian) on Spitsbergen, Svalbard

Jafarian¹,

Groen²,

Nooitgedacht³

et al. 2017

NJG

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Because of outstanding outcrops, Spitsbergen (Svalbard archipelago) provides unique opportunities to investigate the whole Upper Palaeozoic succession in great detail. This study can help to interpret the stratigraphic history and depositional evolution at other locations exposing coeval shelf strata along the northern margin of Pangea, e.g., the southern Barents Sea and Arctic Canada. Bed-scale outcrop observations are combined with microfacies studies to interpret the sedimentary settings and depositional environment of the Upper Palaeozoic strata. A sequencestratigraphic analysis has been carried out to evaluate the relative timing of sediment facies deposition in response to sea-level changes. The Early Artinskian to Kazanian successions of the Templet Member and the Kapp Starostin Formation were divided into five parasequences that are superimposed on a long-term, second-order, sea-level fall. These parasequences record a fundamental change of the sedimentary setting, from a restricted-marine, warm-water carbonate platform to an open-marine, cold-water, biosiliceous-carbonate ramp system. A cross-section across Svalbard comprising nine onshore sections shows that during deposition of the Kapp Starostin Formation a major depocentre marked by thick parasequences and a higher proportion of deep-water facies (bedded cherts) is located in the southwest of Spitsbergen (at Akseløya), whereas northeastern Svalbard records shallow-water microfacies. Svalbard was tectonically passive during the Permian; the local differences in accommodation space and facies were most likely linked to the rejuvenation of pre-existing structural elements, inherited from the Carboniferous. A deepening of the depositional environment combined with cold-water climatic conditions as recorded in our study area has also been documented in other Upper Palaeozoic successions around the Arctic, such as the Finnmark Platform (Norwegian Barents Sea) and the Sverdrup Basin (Arctic Canada). This transition in the depositional environment along the northern margin of Pangea is the result of large-scale changes in oceanic circulation patterns and local palaeogeographic changes during the northward movement of Pangea.

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Late Palaeozoic sequence correlations, North Greenland, Svalbard and the Barents Shelf

Cited by 48 publications

References 20 publications

Tectonic map of the Ellesmerian and Eurekan deformation belts on Svalbard, North Greenland, and the Queen Elizabeth Islands (Canadian Arctic)

Tectonic map of the Ellesmerian and Eurekan deformation belts on Svalbard, North Greenland, and the Queen Elizabeth Islands (Canadian Arctic)

Growth and demise of Permian biogenic chert along northwest Pangea: evidence for end-Permian collapse of thermohaline circulation

Facies arrangement and cyclostratigraphic architecture of the Templet Member and the Kapp Starostin Formation (Permian) on Spitsbergen, Svalbard

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