A brachiopod calcite record of the oceanic carbon and oxygen isotope shifts at the Permian/Triassic transition

Gruszczyński, Michał; Hałas, Stanisław; Hoffman, Antoni; Małkowski, Krzysztof

doi:10.1038/337064a0

Cited by 93 publications

(25 citation statements)

References 21 publications

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“…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). The Kapp Starostin Formation is now seen as passing conformably into the overlying Triassic Vardebukta Formation in the more distal areas (Bugge et al, 1995).…”

Section: Zenith Of Pce: Lopingianmentioning

confidence: 99%

“…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%

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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

267

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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Section: Zenith Of Pce: Lopingianmentioning

confidence: 99%

Section: Expansion Of Pce: Guadalupianmentioning

confidence: 99%

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

Beauchamp

Baud

2002

Palaeogeography, Palaeoclimatology, Palaeoecology

267

132

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“…A sharp decrease to +4 per mil in the C-isotopic curve for the back-reef carbonates equivalent to the upper Capitan (Garber et al, 1989) is consistent with a model involving episodic incursion of alkalinityenriched, 13 C-depleted basinal waters onto the adjacent platform. Other C-isotopic data from numerous localities support the possibility of two or more excursions to less positive values in the late Permian, prior to the epochending drop near the Permo-Triassic boundary (Baud et al, 1989;Gruszczynski et al, 1989;Magaritz et al, 1992;Erwin, 1994). Although the first-order features of the late Permian C-isotopic curve are probably global in nature, smaller negative excursions in individual sections may record local (and hence asynchronous) "burping" of ocean deep water, rather than whole-ocean turnover (well discussed by Kempe and Kazmierczak, 1994).…”

Section: Late Permian Carbonate Precipitation Andmentioning

confidence: 99%

Anomalous Carbonate Precipitates: Is the Precambrian the Key to the Permian?

Grotzinger¹,

Knoll²

1995

PALAIOS

416

215

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“…The PermianÁTriassic boundary at Svalbard has traditionally been placed on the top of the Kapp Starostin Formation, where it is an abrupt change from sandy facies or spiculites to black shales of the Sassendalen Group (Mørk et al 1982;Gruszczyń ski et al 1989;Mørk et al 1989;Mørk et al 1999), producing a distinct recess in the cliff line. Biostratigraphic correlation of different skeletal materials indicates the presence of a hiatus between the Permian and Triassic (sensu Blomeier et al 2011), but preliminary magnetostratigraphic data from central Spitsbergen by Hounslow et al (1996) suggest that the PermianÁTriassic transition is complete, occurring around the formation boundary.…”

Section: Geological Settingmentioning

confidence: 99%

Depositional environment, ichnological features and oxygenation of Permian to earliest Triassic marine sediments in central Spitsbergen, Svalbard

et al. 2016

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A brachiopod calcite record of the oceanic carbon and oxygen isotope shifts at the Permian/Triassic transition

Cited by 93 publications

References 21 publications

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

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

Anomalous Carbonate Precipitates: Is the Precambrian the Key to the Permian?

Depositional environment, ichnological features and oxygenation of Permian to earliest Triassic marine sediments in central Spitsbergen, Svalbard

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