Stable carbon isotope stratigraphy across the Permian–Triassic boundary in shallow marine carbonate platforms, Nanpanjiang Basin, south China

Krull, Evelyn S.; Lehrmann, Daniel J.; Druke, Dominic; Kessel, Benjamin J.; Yu, Yingxin; Li, Rongxi

doi:10.1016/s0031-0182(03)00732-6

Cited by 167 publications

(120 citation statements)

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“…Evidence for a consistent global anomaly of iridium or other rare elements has not been forthcoming for the Permian-Triassic boundary. Nor have abundant and widespread examples of shocked quartz or spherules been found comparable to those at the Cretaceous-Palaeogene boundary, although strong excursions in carbon, oxygen, strontium and sulphur stable isotopes indicating dramatic environmental perturbation have been recorded (Odin et al, 1982;Oberhänsli et al, 1989;Magaritz et al, 1992;Korte et al, 2003;Krull et al, 2004). Despite the scarcity of shocked quartz or platinoid element anomalies, local abundances of meteoritic fragments (Basu et al, 2003) and even a possible impact site, the so called Bedout structure on the Australian northwest continental shelf (Becker et al, 2004), have been used to argue for impact-related extinction at the Permian-Triassic boundary.…”

Section: Discussionmentioning

confidence: 99%

Extinction and recovery patterns of the vegetation across the Cretaceous–Palaeogene boundary — a tool for unravelling the causes of the end-Permian mass-extinction

Vajda

McLoughlin

2007

Review of Palaeobotany and Palynology

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High-resolution palynofloral signatures through the Cretaceous-Palaeogene boundary succession show several features in common with the Permian-Triassic transition but there are also important differences. Southern Hemisphere CretaceousPalaeogene successions, to date studied at high resolution only in New Zealand, reveal a diverse palynoflora abruptly replaced by fungi-dominated assemblages that are in turn succeeded by low diversity suites dominated by fern spores, then gymnosperm-and angiosperm-dominated palynofloras of equivalent diversity to those of the Late Cretaceous. This palynofloral signature is interpreted to represent instantaneous (days to months) destruction of diverse forest communities associated with the Chicxulub impact event. The pattern of palynofloral change suggests wholesale collapse of vascular plant communities and short-term proliferation of saprotrophs followed by relatively rapid successional recovery of pteridophyte and seed-plant communities. The Permian-Triassic transition records global devastation of gymnosperm-dominated forests in a short zone synchronous with one or more peaks of the fungal/algal palynomorph Reduviasporonites. This zone is typically succeeded by assemblages rich in lycophyte spores and/or acritarchs. Higher in the succession, these assemblages give way to diverse palynofloras dominated by new groups of gymnosperms. Although different plant families were involved in the mass-extinctions, the general pattern of extinction and recovery is consistent between both events. The major difference is the longer duration for each phase of the Triassic recovery vegetation compared to that of the Paleocene. The protracted extinction-recovery succession at the Permian-Triassic boundary is incompatible with an instantaneous causal mechanism such as an impact of a celestial body but is consistent with hypotheses invoking extended environmental perturbations through flood-basalt volcanism and release of methane from continental shelf sediments.

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Section: Discussionmentioning

confidence: 99%

Extinction and recovery patterns of the vegetation across the Cretaceous–Palaeogene boundary — a tool for unravelling the causes of the end-Permian mass-extinction

Vajda

McLoughlin

2007

Review of Palaeobotany and Palynology

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“…Globally correlatable excursions in marine d 13 C carb records are often thought to be related to global changes in the carbon cycle, such as those induced by snowball Earth events in the Neoproterozoic [1][2][3] , the oxygenation of Earth's atmosphere [4][5][6][7] , the evolution of Ediacaran metazoans 8,9 , as well as marine and terrestrial extinction episodes [10][11][12][13][14] . A common approach used to establish whether the variations in a d 13 C carb record reflect changes in the isotopic composition of the ancient dissolved inorganic carbon pool is to assess the covariation between coeval carbonate and sedimentary organic carbon isotope records [15][16][17][18][19][20][21][22] . Classically, covariant d 13 C carb and d 13 C org records are interpreted as evidence that both the carbonate and organic matter were originally produced in the surface waters of the ocean, and that they have retained their original d 13 C composition 10,[19][20][21][22][23][24][25] , while decoupled d 13 C carb and d 13 C org records have been interpreted as evidence for diagenetic alteration 16,19,20,26 , the 'Rothman ocean' model 27 , or that local syn-sedimentary processes have made the d 13 C org record noisy 8 .…”

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confidence: 99%

Interpreting carbonate and organic carbon isotope covariance in the sedimentary record

2014

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Many negative d 13 C excursions in marine carbonates from the geological record are interpreted to record significant biogeochemical events in early Earth history. The assumption that no post-depositional processes can simultaneously alter carbonate and organic d 13 C values towards more negative values is the cornerstone of this approach. However, the effects of post-depositional alteration on the relationship between carbonate and organic d 13 C values have not been directly evaluated. Here we present paired carbonate and organic d 13 C records that exhibit a coupled negative excursion resulting from multiple periods of meteoric alteration of the carbonate d 13 C record, and consequent contributions of isotopically negative terrestrial organic matter to the sedimentary record. The possibility that carbonate and organic d 13 C records can be simultaneously shifted towards lower d 13 C values during periods of subaerial exposure may necessitate the reappraisal of some of the d 13 C anomalies associated with noteworthy biogeochemical events throughout Earth history.

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“…However, Liu et al (2006) reported H. parvus at the base of the microbialite in other sites; it is possible that the base of the microbialite, sharply overlying the Changhsing Formation, is indeed the PTB in this site, but this requires further precise stratigraphic work to confirm. Therefore the biostratigraphic Permian-Triassic boundary here is not well-constrained at Laolongdong, so the key horizon in this analysis is the "event horizon" (Krull et al 2004), identified by the base of the microbialite in this section.…”

Section: Locality Geological Setting and Methodsmentioning

confidence: 99%

“…Krull et al, 2004;Payne et al, 2004), attributed to several possible causes associated with the end-Permian mass extinction event (see Erwin, 2006 for review). This sharp change in carbon isotopes is superimposed on a steady decline through the Late Permian (e.g.…”

Section: Introductionmentioning

confidence: 99%

“…Haas et al, 2006), and the prominent shift coincides with the PTB "event horizon", the sharp facies change marking the mass extinction. The event horizon occurs lower than the biostratigraphic Permian-Triassic boundary defined by the conodont Hindeodus parvus (see Krull et al 2004). Microbialites are widespread either on, or a short distance above, the event horizon, including prominent examples in the South China Block (SCB).…”

Section: Introductionmentioning

confidence: 99%

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High-resolution carbon isotope changes in the Permian–Triassic boundary interval, Chongqing, South China; implications for control and growth of earliest Triassic microbialites

Kershaw

et al. 2009

Journal of Asian Earth Sciences

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High-resolution δ 13 C CARB analysis of the Permian-Triassic boundary (PTB) interval at the Laolongdong section, Beibei, near the city of Chongqing, south China, encompasses the latest Permian and earliest Triassic major facies changes in the South China Block (SCB). Microbialites form a distinctive unit in the lowermost 190 cm above the top of the Changhsing Formation (latest Permian) at Laolongdong, comparable to a range of earliest Triassic sites in low latitudes in the Tethyan area. The data show that declining values of δ 13 C CARB , well-known globally, began at the base of the microbialite. High positive values (+3-4 ppt) of δ 13 C CARB in the Late Permian are interpreted to indicate storage of 12 C in the deep waters of a stratified ocean, that was released during ocean overturn in the earliest Triassic, contributing to the distinctive fall in isotope values; this interpretation has been stated by other authors and is followed here. The δ 13 C CARB curve shows fluctuations within the microbialite unit, which are not reflected in the microbialite structure. Comparisons between microbialite branches and adjacent micritic sediment show little difference in δ 13 C CARB , demonstrating that the microbialite grew in equilibrium with surrounding seawater. The Early Triassic microbialites are interpreted to be a response to upwelling of bicarbonate-rich poorly-oxygenated water in low latitudes of Tethys ocean, consistent with current ocean models for the PTB interval. However, the decline of δ 13 C CARB may be due to a combination of processes, including productivity collapse resulting from mass extinction, return of deep water to ocean surface,

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Stable carbon isotope stratigraphy across the Permian–Triassic boundary in shallow marine carbonate platforms, Nanpanjiang Basin, south China

Cited by 167 publications

References 63 publications

Extinction and recovery patterns of the vegetation across the Cretaceous–Palaeogene boundary — a tool for unravelling the causes of the end-Permian mass-extinction

Extinction and recovery patterns of the vegetation across the Cretaceous–Palaeogene boundary — a tool for unravelling the causes of the end-Permian mass-extinction

Interpreting carbonate and organic carbon isotope covariance in the sedimentary record

High-resolution carbon isotope changes in the Permian–Triassic boundary interval, Chongqing, South China; implications for control and growth of earliest Triassic microbialites

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