Differential severity of Permian–Triassic environmental changes on Tethyan shallow-water carbonate platforms

Weidlich, Oliver; Bernecker, Michaela

doi:10.1016/j.gloplacha.2006.06.014

Cited by 39 publications

(20 citation statements)

References 49 publications

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“…Despite many studies, debate continues about the causes of the crisis (Erwin, 2006). Although biodiversity changes have been studied extensively, knowledge of changes in carbonate platforms is less well‐known, yet the carbonate sequences provide high‐resolution archives of marine environmental change (Weidlich & Bernecker, 2007). Carbonate platforms show drastic facies change across the Permian–Triassic boundary (PTB) interval, with subsequent development of thin (up to 40 m thick in places) microbialite carbonate sheets (Baud et al.…”

Section: Introductionmentioning

confidence: 99%

Facies changes and diagenetic processes across the Permian–Triassic boundary event horizon, Great Bank of Guizhou, South China: a controversy of erosion and dissolution

Collin¹,

Kershaw

Crasquin

et al. 2009

Sedimentology

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The Permian–Triassic boundary interval in shallow shelf seas of South China shows Upper Permian limestones overlain by lowermost Triassic microbialites. Global sea‐level rose across the Permian–Triassic boundary, but an irregular top‐Permian erosion surface across a 10 km north–south transect of the Great Bank of Guizhou contains evidence of sea‐level fluctuation. The surface represents the ‘event horizon’ of mass extinction, below the biostratigraphic Permian–Triassic boundary defined by first appearance datum of conodont Hindeodus parvus. An Upper Permian foraminiferal grainstone beneath this surface contains geopetal sediments, etched grains, and pendent and meniscus cements interpreted here as vadose. However, these latter diagenetic processes occurred before the event horizon and were followed by erosion of the final Permian surface. This erosion cuts previous fabrics but lacks evidence of weathering or bioerosion. A few centimetres below is an earlier grainstone that was also eroded but lacks proof of sub‐aerial processes. Samples therefore reveal one, or possibly two, small‐scale relative sea‐level changes before the Triassic transgression in this area, and these may relate to local tectonics. The final Permian surface is subject to at least four interpretations: (i) sub‐aerial physical erosion and dissolution by carbon dioxide‐enriched fresh water or carbon dioxide‐enriched mixed water, prior to Triassic transgression; (ii) sub‐aerial physical erosion overprinted by dissolution related to carbon dioxide‐enriched sea water in the Early Triassic transgression; (iii) submarine dissolution affected by acidified sea water due to rapid increase in volcanically‐derived carbon dioxide and oxidized methane released from marine clathrates; (iv) submarine dissolution due to acid anoxic waters rising across the continental shelf, unrelated to atmospheric carbon dioxide or oxidized methane. Field and petrographic evidence suggests that (i) is the simplest option; and it is possible that (ii) and (iii) occurred, but none are proved. Option (iv) is unlikely given the evidence and modelling of supersaturation of upwelled waters with respect to bicarbonate.

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Section: Introductionmentioning

confidence: 99%

Facies changes and diagenetic processes across the Permian–Triassic boundary event horizon, Great Bank of Guizhou, South China: a controversy of erosion and dissolution

Collin¹,

Kershaw

Crasquin

et al. 2009

Sedimentology

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“…The Upper Permian to Middle Triassic Ru'us al Jibal Group encompasses the Bih, Hagil and Ghail formations, whereas the Upper Triassic Elphinstone Group comprises the Milaha and Ghalilah formations. The Permian–Triassic carbonate rocks of the Saiq Plateau (Al Jabal al‐Akhdar, Oman) were studied by Weidlich & Bernecker (, ) and Koehrer et al . (, ).…”

Section: Geological Settingmentioning

confidence: 99%

Fluid–rock interactions associated with regional tectonics and basin evolution

et al. 2013

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An integrated approach consisting of fracture analysis, petrography, carbon, oxygen and strontium-isotope analyses, as well as fluid-inclusion micro-thermometry, led to a better understanding of the evolution of fluid-rock interactions and diagenesis of the Upper Permian to Upper Triassic carbonates of the United Arab Emirates. The deposited carbonates were first marked by extensive early dolomitization. During progressive burial, the carbonates were affected by dolomite recrystallization as well as precipitation of vug and fracture-filling dolomite, quartz and calcite cements. After considerable burial during the Middle Cretaceous, sub-vertical north-south oriented fractures (F1) were cemented by dolomite derived from mesosaline to hypersaline fluids. Upon the Late Cretaceous maximum burial and ophiolite obduction, sub-vertical east-west fractures (F2) were cemented by dolomite (Dc2) and saddle dolomite (Ds) derived from hot, highly saline fluids. Then, minor quartz cement has precipitated in fractures from hydrothermal brines. Fluid-inclusion analyses of the various diagenetic phases imply the involvement of increasingly hot (200°C) saline brines (20 to 23% NaCl eq.). Through one-dimensional burial history numerical modelling, the maximum temperatures reached by the studied rocks are estimated to be in the range of 160 to 200°C. Tectonically-driven flux of hot fluids and associated diagenetic products are interpreted to have initiated during the Late Cretaceous maximum burial and lasted until the Oligocene-Miocene compressional tectonics and related uplift. The circulation of such hydrothermal brines led to partial dissolution of dolomites (Dc2 and Ds) and to precipitation of hydrothermal calcite C1 in new (mainly oriented north-south; F3) and preexisting, reactivated fractures. The integration of the obtained data confirms that the diagenetic evolution was controlled primarily by the interplay of the burial thermal evolution of the basin and the regional tectonic history. Hence, this contribution highlights the impacts of regional tectonics and basin history on diagenetic processes, which may subsequently affect reservoir properties.

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“…In the Wadi Wasit area, this red cephalopod-bearing carbonate unit (Blendinger, 1988;Pillevuit et al, 1997;Baud et al, 2001b;Richoz et al, 2010) is overlain by nodular, cherty and turbiditic (allodapic) limestone. After a stratigraphic gap of nearly 10 Myrs, the Lower Triassic record begins with Dienerian breccias containing reworked blocks of Middle Permian to basal Triassic platform carbonate (Béchennec et al, 1992b;Pillevuit, 1993;Pillevuit et al, 1997;Weidlich and Bernecker, 2007;Krystyn et al, 2003;Twitchett et al, 2004;Richoz et al, 2010). In close proximity to tilted blocks or isolated as distal plateaus, all of these Permian basinal sediments lay above the Calcite Compensation Depth (CCD) and are overlain by clastic carbonate, breccia or debris flows of Late Permian or Early Triassic age.…”

Section: Comparison With Other Permian Basinal Facies Known In the Hamentioning

confidence: 99%

The Buday’ah Formation, Sultanate of Oman: A Middle Permian to Early Triassic oceanic record of the Neotethys and the late Induan microsphere bloom

Baud

Richoz

Beauchamp

et al. 2012

Journal of Asian Earth Sciences

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Keywords:Permian Lower Triassic Chert Radiolaria Conodonts Chemostratigraphy Platy and papery limestone a b s t r a c tThe Middle Permian to Lower Triassic Buday'ah section, exposed in the Oman Mountains, is the first deepsea section to be described in the Neotethys. The oceanic sediments were deposited along the southern Tethys margin in the newly formed Hawasina Basin. It is one of the few places where true Tethyan Permian radiolarites are exposed that allow the documentation of CCD evolution through time. The succession begins as oceanic crust pillow basalt with red ammonoid-rich pelagic limestone occurring both above and within inter-pillow cavities; the new occurrence of Clarkina postbitteri hongshuiensis indicates a late Capitanian age for the carbonate. The sharp change to overlying late Capitanian to Changhsingian radiolarite reflects rapid subsidence about 10 Myrs after initial continental breakup that resulted in the formation of the Neotethys Ocean. New conodonts indicate that the Permian-Triassic boundary succession occurs in the first platy lime mudstone beds above a Changhsingian siliceous to calcareous shale unit. The platy lime mudstone beds include an Upper Griesbachian bloom of calcite filled spheres (radiolarians?) that marks a potential world-wide event. New conodonts indicate an early Olenekian age for overlying grey papery limestone that are devoid of both macrofossils and trace fossils indicating that recovery from the Late Permian extinction has not yet progressed within this deep-water environment.d 13 C org , isotope values have not been disturbed and they show a negative shift just below the PermianTriassic transition and a second one at the parvus zone level above. The Buday'ah succession may represent the most distal and probably deepest Permian and Lower Triassic depositional sequence within the basin.

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Differential severity of Permian–Triassic environmental changes on Tethyan shallow-water carbonate platforms

Cited by 39 publications

References 49 publications

Facies changes and diagenetic processes across the Permian–Triassic boundary event horizon, Great Bank of Guizhou, South China: a controversy of erosion and dissolution

Facies changes and diagenetic processes across the Permian–Triassic boundary event horizon, Great Bank of Guizhou, South China: a controversy of erosion and dissolution

Fluid–rock interactions associated with regional tectonics and basin evolution

The Buday’ah Formation, Sultanate of Oman: A Middle Permian to Early Triassic oceanic record of the Neotethys and the late Induan microsphere bloom

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