Pangea and the Paleogeography of the Permian

Scotese, Christopher R.; Langford, Richard P.

doi:10.1007/978-3-642-78593-1_1

Cited by 133 publications

(80 citation statements)

References 22 publications

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“…To some extent, this cooling can be associated with the northward migration of Pangea during the Late Palaeozoic. Various reconstructions (Golonka et al, 1994;Scotese and Langford, 1995;Ziegler et al, 1998;Golonka and Ford, 2000) show that the Sverdrup Basin migrated from about 25 ‡N during the Late Carboniferous to about 40 ‡N during the Early Triassic (Fig. 1).…”

Section: Permian Coolingmentioning

confidence: 98%

“…Likewise, cold oceanic upwelling was the explanation o¡ered by Murchey and Jones (1992) for the origin of the PCE and its association with phosphate-rich deposits along western North America. Accordingly, eastward-directed upwelling, resulting from Coriolis-driven wind-forcing along the western continental margin of Pangea, is a plausible explanation, since the area was in the northern hemisphere from the Early Carboniferous onward (Scotese and Langford, 1995). A northern gyre would have also generated a southbound sur¢cial current akin to the modern California Current and would have brought cold waters all along northwest Pangea (Fig.…”

Section: Thermohaline Circulationmentioning

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: Permian Coolingmentioning

confidence: 98%

Section: Thermohaline Circulationmentioning

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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“…The Tethys region is certainly on of the most complex regions in Pangea (Scotese and Lanford, 1995) and there is no consensus regarding the number, extent, and configuration of the different crustal blocks that crossed the Tethys at the end of the Palaeozoic (Nie et al, 1990). Despite these problems, several interesting recent Late Pennian palaeogeographic reconstructions including the Iberian Plate have appeared in the literature (see Ziegler, 1988Ziegler, , 1990Ziegler, , 1993Ziegler and Stampfli, 2001 ;Stampfli and Borel, 2002;Stampfli et aI., 2001 ;Ford and Golonka, 2003 ;Ronov et aI., 1984, among others).…”

Section: Palaeogeographymentioning

confidence: 99%

“…Among other variables, these models include patterns of surface temperature, precipitation and evaporation balance and sea-level pressure parameters and have provided data on the role of continental configumtion as a climateforcing factor (Barron and Facett, 1995 A simple view of the latitudinal location and the topography of the Iberian Plate shown in the different global palaeogeographical maps for the Late Permian-PTB times (see for example Ziegler, 1988;Ziegler and Stampfli, 2001;Stampfli and Bore!, 2002) clearly allows us to infer a few basic palaeoclimatie characteristics for this western Tethysian area. The Iberian Plate was part of the Central Pangean Mountain Range, made up of the Appalachian-Mauretanide-Variscan orogenic belts that fonned as a result of the diachronous collision between Laurasia and Gondwana (Scotese and Lanford, 1995). This mountain belt, extending across the southeastern seaboard of North America and into western Africa (Mauritania) and northermnost South America, was highest during the Early Permian and had already begun to collapse during the Late Permian.…”

Section: During Latest Pennian-earliest Triassic Times Thementioning

confidence: 99%

Stratigraphical and palaeogeographical significance of the continental sedimentary transition across the Permian–Triassic boundary in Spain

López-Gómez¹,

Arché²,

Marzo

et al. 2005

Palaeogeography, Palaeoclimatology, Palaeoecology

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“…The Delaware Basin was situated close to the western margin of Pangaea during Guadalupian times and lay about 10°n orth of the paleo-equator of that time (Scotese & McKerrow 1990;Scotese & Langford 1995). The region consisted of a series of carbonate shelves and platforms (Kerans & Kempter 2002).…”

Section: Sand Sourcesmentioning

confidence: 99%

Role of sea-level change in deep water deposition along a carbonate shelf margin, Early and Middle Permian, Delaware Basin: implications for reservoir characterization

Li¹,

Yu²,

Li³

et al. 2015

Geologica Carpathica

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Abstract:The architecture and sedimentary characteristics of deep water deposition can reflect influences of sea-level change on depositional processes on the shelf edge, slope, and basin floor. Outcrops of the northern slope and basin floor of the Delaware Basin in west Texas are progressively exposed due to canyon incision and road cutting. The outcrops in the Delaware Basin were measured to characterize gravity flow deposits in deep water of the basin. Subsurface data from the East Ford and Red Tank fields in the central and northeastern Delaware Basin were used to study reservoir architectures and properties. Depositional models of deep water gravity flows at different stages of sea-level change were constructed on the basis of outcrop and subsurface data. In the falling-stage system tracts, sandy debris with collapses of reef carbonates are deposited on the slope, and high-density turbidites on the slope toe and basin floor. In the low-stand system tracts, deep water fans that consist of mixed sand/mud facies on the basin floor are comprised of high-to low-density turbidites. In the transgression and high-stand system tracts, channel-levee systems and elongate lobes of mud-rich calciturbidite deposits formed as a result of sea level rise and scarcity of sandy sediment supply. For the reservoir architecture, the fan-like debris and high-density turbidites show high net-to-gross ratio of 62 %, which indicates the sandiest reservoirs for hydrocarbon accumulation. Lobe-like deep water fans with net-to-gross ratio of 57 % facilitate the formation of high quality sandy reservoirs. The channel-levee systems with muddy calciturbidites have low net-to-gross ratio of 30 %.

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Pangea and the Paleogeography of the Permian

Cited by 133 publications

References 22 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

Stratigraphical and palaeogeographical significance of the continental sedimentary transition across the Permian–Triassic boundary in Spain

Role of sea-level change in deep water deposition along a carbonate shelf margin, Early and Middle Permian, Delaware Basin: implications for reservoir characterization

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