Intensified chemical weathering during the Permian-Triassic transition recorded in terrestrial and marine successions

Cao, Ying; Song, Huyue; Algeo, Thomas J.; Chu, Daoliang; Du, Yong; Tian, Li; Wang, Yuhang; Tong, Jinnan

doi:10.1016/j.palaeo.2018.06.012

Cited by 84 publications

(31 citation statements)

References 104 publications

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Section: Discussionmentioning

confidence: 70%

“…In addition, the intensifying weathering and aridity through the terrestrial Permian-Triassic strata in North China are confirmed by geochemical data (Cao et al, 2019;Zhu et al, 2019a). Multiple weathering indexes [for example, Chemical Index of Alteration (CIA), Chemical Index of Weathering (CIW) and Plagioclase Index of Alteration (PIA)] and clay minerals all suggest increasingly intense weathering (a major excursion towards higher values) around the PTB in North China (Cao et al, 2019;Zhu et al, 2019a) and South China (Xu et al, 2017a,b). A similar greater intensity in weathering and increasing aridity were also confirmed in the Karoo Basin of South Africa (Ward et al, 2000;Retallack et al, 2003), Russia (Newell et al, 1999(Newell et al, , 2010, the Iberian Ranges of Spain (Mujal et al, 2017(Mujal et al, , 2018 and the North Sea (P eron et al, 2005;Bourquin et al, 2011;Wilson et al, 2019).…”

Section: Discussionmentioning

confidence: 70%

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Intensifying aeolian activity following the end‐Permian mass extinction: Evidence from the Late Permian–Early Triassic terrestrial sedimentary record of the Ordos Basin, North China

et al. 2020

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Sedimentary successions provide direct evidence of climate and tectonics, and these give clues about the causes of the mass extinction around the Permian–Triassic boundary. Terrestrial Permian–Triassic boundary strata in the eastern Ordos Basin, North China, include the Late Permian Sunjiagou, Early Triassic Liujiagou and late Early Triassic Heshanggou formations in ascending order. The Sunjiagou Formation comprises cross‐bedded sandstones overlaid by mudstones, indicating meandering rivers with channel, point bar and floodplain deposits. The Liujiagou Formation was formed in braided rivers of arid sand bars interacting with some aeolian dune deposits, distinguished by abundant sandstones where diverse trough and planar cross‐bedding and aeolian structures (for example, inverse climbing‐ripple, translatent‐ripple lamination, grainfall and grainflow laminations) interchange vertically and laterally. The Heshanggou Formation is a rhythmic succession of mudstones interbedded with thin medium‐grained sandstones mainly deposited in a shallow lacustrine environment. Overall, the sharp meandering to braided to shallow lake sedimentary transition documents palaeoenvironmental changes from semi‐arid to arid and then to semi‐humid conditions across the Permian–Triassic boundary. The die‐off of tetrapods and plants, decreased bioturbation levels in the uppermost Sunjiagou Formation, and the bloom of microbially‐induced sedimentary structures in the Liujiagou Formation marks the mass extinction around the Permian–Triassic boundary. The disappearance of microbially‐induced sedimentary structures, increasingly intense bioturbation from bottom to top and the reoccurrence of reptile footprints in the Heshanggou Formation reveal gradual recovery of the ecosystem after the Permian–Triassic boundary extinction. This study is the first to identify the intensification of aeolian activity following the end‐Permian mass extinction in North China. Moreover, while northern North China continued to be uplifted tectonically from the Late Palaeozoic to Late Mesozoic, the switch of sedimentary patterns across the Permian–Triassic boundary in Shanxi is largely linked to the development of an arid and subsequently semi‐humid climate condition, which probably directly affected the collapse and delayed recovery in palaeoecosystems.

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Section: Discussionmentioning

confidence: 70%

Section: Discussionmentioning

confidence: 70%

Intensifying aeolian activity following the end‐Permian mass extinction: Evidence from the Late Permian–Early Triassic terrestrial sedimentary record of the Ordos Basin, North China

et al. 2020

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“…In recent years, various investigations of chemical weathering indices and especially the CIA, have been successfully used to quantify the chemical weathering degree of provenance area and thus constrain deep-time palaeoclimatic variation (e.g., Paikaray et al 2008;Yang and Du 2017;Cao et al 2019;Chaudhuri et al 2020). Xu and Shao (2018) proposed that the influences of sedimentary differentiation through grain size differences, sediment recycling, further weathering in sedimentary regions, pedogenesis and potassium metasomatism should be taken into account before estimating the chemical weathering intensity in the provenance area.…”

Section: Evaluating Influence Factors Of Chemical Weathering Indicesmentioning

confidence: 99%

“…The compositions of sediments are closely related to the signature of the source area (Cullers 1994(Cullers , 2000. It is necessary to show that samples have a unified protolith in order to describe palaeoclimate characteristics based on variations of chemical weathering (Cao et al 2019). In this study, the mudstone samples of the Shahai and Fuxin formations originated from the same type of provenance close to the Fuxin Basin, which results in the similar chemical weathering degrees between provenance Fig.…”

Section: Interpretation Of Chemical Weathering Fluctuationsmentioning

confidence: 99%

Continental chemical weathering during the Early Cretaceous Oceanic Anoxic Event (OAE1b): a case study from the Fuxin fluvio-lacustrine basin, Liaoning Province, NE China

Shao

Lan

et al. 2020

J. Palaeogeogr.

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This study focuses on Early Cretaceous mudstones from the Shahai and Fuxin formations in the Fuxin continental basin. We analyse chemical weathering, land surface temperatures and palaeoclimates based on chemical weathering indices, and emphasize the implications of continental chemical weathering on nutrient fluxes into lakes and oceans. According to Cr and Ni abundance, Al 2 O 3-TiO 2 , La/Sc-Th/Co and V-Ni-Th×10 plots, as well as rare earth element (REE) analysis, mudstone samples from the Shahai and Fuxin formations were derived from the same type of provenance comprising mainly felsic igneous rocks. Chemical weathering trends reflected by the Chemical Index of Alteration (CIA), Weathering Index of Parker (WIP) and the Mafic Index of Alteration for Oxidative weathering environments (MIA (O)) are consistent with each other and allow the geological succession to be divided into four stages. Land surface temperatures of the Shahai and Fuxin formations are estimated based on the linear relationship of CIA to temperature, and also can be divided into four stages consistent with those determined from chemical weathering trends. During Stage A (early part of the late Aptian) chemical weathering and land surface temperatures were relatively low and showed characteristic high fluctuations, while Stage B (latest Aptian) represented a transitional period where weathering rates and temperatures increased, and high amplitude fluctuations continued. Conditions changed markedly in Stage C (early Albian) with very high and stable weathering, and warm, humid climates, while in Stage D (middle and late Albian) conditions returned to low chemical weathering and land surface temperatures. These stages of chemical weathering and land surface temperature fluctuations represent responses to global climate fluctuations during the Early Cretaceous, with the early Albian high weathering intensities and warm, humid climates combining to create high nutrient levels that would have flushed through rivers into lakes and ultimately oceans. This correlates stratigraphically with the development of Early Cretaceous black shales during Ocean Anoxic Event 1b, showing the importance of continental weathering regimes as a causal mechanism for lake and ocean anoxia.

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“…More than 90% of all marine species and >70% of terrestrial species were eliminated during the crisis (Raup 1979; Erwin 1993; Jin et al 2000; Benton 2003; Song et al 2013), leading to the “reef gap” (Flügel and Kiessling 2002; Kiessling et al 2010), a flat latitudinal biodiversity gradient (Song et al 2020), and a reversed functional pyramid in the Early Triassic oceans (Song et al 2018). Many kinds of (often synergistic) environmental stresses have been implicated in the crisis, including global warming (Kidder and Worsley 2004; Joachimski et al 2012; Sun et al 2012), hypercapnia (Knoll et al 1996, 2007), oceanic anoxia (Wignall and Hallam 1992; Wignall and Twitchett 1996, 2002; Grice et al 2005; Kump et al 2005; Shen et al 2007; Brennecka et al 2011; Song et al 2011; Lau et al 2016; Penn et al 2018; Huang et al 2019), oceanic acidification (Liang 2002; Hinojosa et al 2012; Clarkson et al 2015), increased siltation (Algeo and Twitchett 2010) and turbidity (Cao et al 2019), ozone depletion (Visscher et al 2004; Beerling et al 2007; Black et al 2014; Bond et al 2017), toxic metal poisoning (Wang 2007; Sanei et al 2012), and more (Racki and Wignall 2005; Reichow et al 2009).…”

Section: Introductionmentioning

confidence: 99%

Size variations in foraminifers from the early Permian to the Late Triassic: implications for the Guadalupian–Lopingian and the Permian–Triassic mass extinctions

Feng¹,

Song²,

Bond³

2020

Paleobiology

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The final 10 Myr of the Paleozoic saw two of the biggest biological crises in Earth history: the middlePermian extinction (often termed the Guadalupian–Lopingian extinction [GLE]) that was followed 7–8 Myr later by Earth's most catastrophic loss of diversity, the Permian–Triassic mass extinction (PTME). These crises are not only manifest as sharp decreases in biodiversity and—particularly for the PTME—total ecosystem collapse, but they also drove major changes in biological morphological characteristics such as the Lilliput effect. The evolution of test size among different clades of foraminifera during these two extinction events has been less studied. We analyzed a global database of foraminiferal test size (volume) including 20,226 specimens in 464 genera, 98 families, and 9 suborders from 632 publications. Our analyses reveal significant reductions in foraminiferal mean test size across the Guadalupian/Lopingian boundary (GLB) and the Permian/Triassic boundary (PTB), from 8.89 to 7.60 log10 μm3 (lg μm3) and from 7.25 to 5.82 lg μm3, respectively. The decline in test size across the GLB is a function of preferential extinction of genera exhibiting gigantism such as fusulinoidean fusulinids. Other clades show little change in size across the GLB. In contrast, all Lopingian suborders in our analysis (Fusulinina, Lagenina, Miliolina, and Textulariina) experienced a significant decrease in test size across the PTB, mainly due to size-biased extinction and within-lineage change. The PTME was clearly a major catastrophe that affected many groups simultaneously, and the GLE was more selective, perhaps hinting at a subtler, less extreme driver than the later PTME.

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Intensified chemical weathering during the Permian-Triassic transition recorded in terrestrial and marine successions

Cited by 84 publications

References 104 publications

Intensifying aeolian activity following the end‐Permian mass extinction: Evidence from the Late Permian–Early Triassic terrestrial sedimentary record of the Ordos Basin, North China

Intensifying aeolian activity following the end‐Permian mass extinction: Evidence from the Late Permian–Early Triassic terrestrial sedimentary record of the Ordos Basin, North China

Continental chemical weathering during the Early Cretaceous Oceanic Anoxic Event (OAE1b): a case study from the Fuxin fluvio-lacustrine basin, Liaoning Province, NE China

Size variations in foraminifers from the early Permian to the Late Triassic: implications for the Guadalupian–Lopingian and the Permian–Triassic mass extinctions

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