New Early to Middle Triassic U–Pb ages from South China: Calibration with ammonoid biochronozones and implications for the timing of the Triassic biotic recovery

Ovtcharova, Maria; Bucher, Hugo; Schaltegger, Urs; Galfetti, Thomas; Brayard, Arnaud; Guex, Jean

doi:10.1016/j.epsl.2006.01.042

Cited by 210 publications

(136 citation statements)

References 32 publications

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“…1, Inset from this study and Cao et al (11). Remainder of carbonate carbon isotopic composition from Payne et al (52) and geochronology from Galfetti et al (54). Permian and Triassic conodont zones from Ogg et al (63).…”

mentioning

confidence: 99%

High-precision timeline for Earth’s most severe extinction

Burgess

Bowring

Shen

2014

Proc. Natl. Acad. Sci. U.S.A.

599

479

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Significance Mass extinctions are major drivers of macroevolutionary change and mark fundamental transitions in the history of life, yet the feedbacks between environmental perturbation and biological response, which occur on submillennial timescales, are poorly understood. We present a high-precision age model for the end-Permian mass extinction, which was the most severe loss of marine and terrestrial biota in the last 542 My, that allows exploration of the sequence of events at millennial to decamillenial timescales 252 Mya. This record is critical for a better understanding of the punctuated nature and duration of the extinction, the reorganization of the carbon cycle, and a refined evaluation of potential trigger and kill mechanisms.

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mentioning

confidence: 99%

High-precision timeline for Earth’s most severe extinction

Burgess

Bowring

Shen

2014

Proc. Natl. Acad. Sci. U.S.A.

599

479

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“…U-Pb dating of perovskites in the early Arydzhangsky flow and zircons from the late Delkansky silicic tuff of extrusive suites in the Maymecha-Kotuy region suggests that the STLIP flood basalt eruptions commenced at 251.7 ± 0.4 Ma and ended at 251.1 ± 0.3 Ma, i.e., representing an interval of ∼ 600 kyr (Renne et al, 1995;Kamo et al, 2003). However, an Ar-Ar date of 250.3 ± 1.1 Ma was obtained for the final stage of extrusive volcanism at Norilsk, the core area of the STLIP (Reichow et al, 2009; see also the review of evidence for a late eruptive stage by Ovtcharova et al, 2006). The more critical issue, in any case, is the duration not of flood basalt eruptions but of intrusive magmatism in the West Siberian Coal Basin, which was probably the main source of volcanogenic greenhouse gases (Retallack and Jahren, 2008;Black et al, 2012).…”

Section: Causes and Consequences Of The Ssb Eventmentioning

confidence: 99%

“…Age constraints were provided by chemical abrasion-thermal ionization mass spectrometry (CA-TIMS) studies of U-Pb in zircons, from which the dates of the Induan-Olenekian and SmithianSpathian boundaries were estimated at ∼ 251.25 Ma and ∼ 250.55 Ma, respectively (Ovtcharova et al, 2006), and that of the Olenekian-Anisian boundary was estimated at ∼ 247.3 Ma . These dates yield durations for the Smithian and Spathian substages of ∼ 0.7 and ∼ 3.25 Myr, respectively.…”

Section: Age Model and Sediment Flux Calculationsmentioning

confidence: 99%

Amelioration of marine environments at the Smithian–Spathian boundary, Early Triassic

et al. 2015

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Abstract. The protracted recovery of marine ecosystems following the Permian-Triassic mass extinction may have been caused, in part, by episodic environmental and climatic crises during the Early Triassic, among which the SmithianSpathian boundary (SSB) event is conspicuous. Here, we investigate the SSB event in the Shitouzhai section, Guizhou Province, South China, using a combination of carbonate carbon (δ 13 C carb ) and carbonate-associated sulfate sulfur isotopes (δ 34 S CAS ), rare earth elements, and elemental paleoredox and paleoproductivity proxies. The SSB at Shitouzhai is characterized by a +4 ‰ shift in δ 13 C carb and a −10 to −15 ‰ shift in δ 34 S CAS , recording negative covariation that diverges from the positive δ 13 C carb -δ 34 S CAS covariation that characterizes most of the Early Triassic. This pattern is inferred to reflect an increase in organic carbon burial (e.g., due to elevated marine productivity) concurrently with the oxidation of isotopically light H 2 S, as the result of enhanced vertical advection of nutrient-and sulfide-rich deep waters to the ocean-surface layer. Enhanced upwelling was likely a response to climatic cooling and the reinvigoration of globalocean overturning circulation at the SSB. Coeval decreases in chemical weathering intensity and detrital sediment flux at Shitouzhai are also consistent with climatic cooling. A decline in marine biodiversity was probably associated with the late Smithian thermal maximum (LSTM) rather than with the SSB per se. The SSB thus marked the termination of the extreme hothouse conditions of the GriesbachianSmithian substages of the Early Triassic and is significant as a record of accompanying climatic, environmental, and biotic changes. The ultimate cause of the SSB event is uncertain but may have been related to a reduction in intrusive magmatic activity in the Siberian Traps large igneous province.

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“…The Induan-Olenekian boundary is dated at 251.3 Ma by Mundil et al (2010) and at 251.22 ± 0.20 Ma (Ovtcharova et al, 2006;Burgess et al, 2014) but at 250.00 Ma in the new Geologic Timescale 2012 . The new younger age for this boundary in Gradstein et al (2012) is based on cyclo/magnetostratigraphy and ammonoid data.…”

Section: Induan-olenekian Boundarymentioning

confidence: 99%