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Different Triggers for the Two Pulses of Mass Extinction Across the Permian

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Different Triggers for the Two Pulses of Mass Extinction Across the Permian www.nature.com/scientificreports OPEN Diferent triggers for the two pulses of mass extinction across the Permian and Triassic boundary Guoshan Li1,2, Wei Liao2,3, Sheng Li2,4, Yongbiao Wang2* & Zhongping Lai1* Widespread ocean anoxia has been proposed to cause biotic mass extinction across the Permian– Triassic (P–Tr) boundary. However, its temporal dynamics during this crisis period are unclear. The Liangfengya section in the South China Block contains continuous marine sedimentary and fossil records. Two pulses of biotic extinction and two mass extinction horizons (MEH 1 & 2) near the P– Tr boundary were identifed and defned based on lithology and fossils from the section. The data showed that the two pulses of extinction have diferent environmental triggers. The frst pulse occurred during the latest Permian, characterized by disappearance of algae, large foraminifers, and fusulinids. Approaching the MEH 1, multiple layers of volcanic clay and yellowish micritic limestone occurred, suggesting intense volcanic eruptions and terrigenous infux. The second pulse occurred in the earliest Triassic, characterized by opportunist-dominated communities of low diversity and high abundance, and resulted in a structural marine ecosystem change. The oxygen defciency inferred by pyrite framboid data is associated with biotic declines above the MEH 2, suggesting that the anoxia plays an important role. Abbreviations GSSP Global stratotype section and point MEH Mass extinction horizon PTB Permian–Triassic boundary PTME Permian–Triassic mass extinction SEM Scanning electron microscope SCB South China Block Te Permian–Triassic (P–Tr) mass extinction 1 (~ 252 Ma)2, destroyed both terrestrial and marine life 3 and killed more than 90% of all species on Earth 1,4. Te extinction is the largest and most devastating biotic crisis of the Phanerozoic Aeon5,6 because it caused whole-scale reorganization in marine ecosystems and the transition from the Palaeozoic evolutionary fauna to the Modern evolutionary fauna 7. While the exact causes and the nature of this extinction are unknown6, numerous hypotheses, including episodic volcanism8,9, rapid changes of sea level10, lethally hot temperatures 11, widespread oceanic anoxia 12,13, oceanic acidifcation 14, oceanic toxicity 15, and multiple catastrophic events16 have been proposed. Severe environmental perturbations related to giant volcanic eruptions have recently been considered one of the most likely killing mechanisms9. Oceanic anoxia across the P–Tr boundary is a global event and a major killing mechanism for extinction17. Besides, it explains the protracted recovery afer the extinction18–20. However, the temporal dynamics of anoxia using proxies are still poorly constrained. Various proxies such as sedimentological and palaeoecological features 12, T/U ratios 21, cerium anomaly changes22, molybdenum isotopic composition 23, uranium isotopes from dolostones 24, sulfur isotopic excursions 25, carbon isotopes26, and molecular biomarkers have been used to constrain the timing and nature of marine redox conditions during the crisis interval27. However, the geochemical proxies have several potential interpretations 1Institute of Marine Sciences, Guangdong Provincial Key Laboratory of Marine Biotechnology, Shantou University, Shantou 515063, China. 2School of Earth Sciences, China University of Geosciences (Wuhan), Wuhan 430074, China. 3Anthropology Museum of Guangxi, Nanning 530028, China. 4No.3 Institute of Geological & Mineral Resources Survey of Henan Geological Bureau, Zhengzhou 450000, China. *email: [email protected]; [email protected] Scientifc Reports | (2021) 11:6686 | https://doi.org/10.1038/s41598-021-86111-7 1 Vol.:(0123456789) www.nature.com/scientificreports/ due to diagenesis28, and their applications are ofen limited in scope. Te morphology and size distribution of pyrite framboids, which is a robust redox indicator found in both carbonate and mudstone/shale facies 29, are a reliable proxy of benthic oxygenation in both modern environments 29 and ancient sediments30,31. In the South China Block, a small tectonic plate located in the eastern Tethys where the shallow-water plat- form and deep-water siliceous–argillaceous sedimentary facies coexist, pyrite framboids have been used as an indicator to investigate the P–Tr mass extinction. Numerous studies of pyrite framboid-inferred palaeoredox conditions have focused on deep ocean deposited sedimentary rocks32,33. However, a few have studied shallow platform sediments34,35, where microbialites are ofen bloomed as disaster forms afer the mass extinction. Pre- vious studies have suggested that a long-term and widespread oceanic anoxia occurred during the extinction 13. Mounting evidence show that oceanic redox conditions underwent high-frequency oscillations 24,33,36. Bond and Wignall30 suggested that anoxic conditions in the Palaeotethys were complex and unstable based on size distribu- tions of pyrite framboids from several P–Tr boundary sections. However, those conodont data are not available in many Bond and Wignall sections30 to confrm the P–Tr boundary. Besides, the sampling density is also not high enough to refect palaeoredox changes. Moreover, a depositional hiatus usually exists between conodont Clakina meishanensis and Hindeodus changxingesis zones in the shallow carbonate platform sediments in the South China Block10. Terefore, high-resolution palaeoecologic and sedimentologic studies from consecutive shallow settings are needed to reconstruct detailed oceanic palaeoredox changes during this critical interval. Terefore, high-density and high-resolution samples were collected, and the triggers and pattern of mass extinction from the Liangfengya section were investigated. Tis study helps assess the temporal link between environmental triggers and two pluses of extinction by comparing it with the previous studies in the Yangtze Platform before, during, and afer the mass extinction. Geological and stratigraphic settings Two diferent sedimentary facies coexisted in the South China Block (SCB) during the Changhsingian (Late Permian) [(1) shallow-water platform facies represented by various carbonate-dominated sediments and (2) deep-water siliceous/argillaceous deposits (Fig. 1)]. Te Liangfengya section is located in an abandoned quarry in the Mt. Zhongliang area, 10 km west of Chongqing city, and the upper Yangtze Carbonate Platform (Fig. 1A). Yang et al.37 were the frst to study it and since then it is one of the most important P–Tr boundary sections38. Te Liangfengya area recorded a shallow-water carbonate platform, inter-reef facies deposits during the Late Permian39. Tere are representatives of Late Permian sponge-dominated reef facies in the northeast of Liangfengya40. Tis study analyzed the upper Changxing Formation and the basal Feixianguan Formation of the section (Fig. 1B). Te total thickness of the section is about 6.4 m, with 18 beds (Beds 1–18) (Fig. 2). Te topmost two meters of the upper Permian Changxing Formation, Bed 1, consists of medium to thick, bioclastic limestone, and yields abundant fossil fragments, such as foraminifers and fusulinids 41, calcareous algae42, conodonts38, and calcareous sponges40. Te lower part of the Feixianguan Formation is characterized by alternating yellowish shale and gray marlstones (Beds 2–15). Te frst episode of the mass extinction occurs at the topmost of Bed 8. It is characterized by the disappearance of a fossil assemblage dominated by fusulinids, calcareous algae42, and Permian brachiopods43. Te basal fve meters of the overlying earliest Triassic Feixianguan Formation comprise fne-grained lithologies including micrites and marls. Tin claystone, calcareous shales, and mudstone, sparse fauna separate the lithologies. Beds 9–15 contain a fossil assemblage with low diversity including small fora- minifers, small gastropods, and ostracods. Beds 16–18 have a few bivalves, where pyrite framboids are common. Overall, three fossil assemblage groups suggest a two-pulses extinction event straddling the P–Tr boundary. Conodonts are essential index fossils for P–Tr stratigraphic studies. Yuan and Shen 38 established fve cono- dont biozones within the Liangfengya section based on their occurrence. According to the frst Hindeodus parvus appearance, the P–Tr boundary was placed at 81 cm above the bioclastic limestone of the Changxing Formation38. In this study, samples were collected at an interval of 5 ~ 10 cm from the upper Changxing Forma- tion and lower Feixianguan Formation to conduct a high-resolution conodont stratigraphic study. Conodont H. parvus appeared in sample LFY 10-2 of Bed 10 (Fig. 1C), indicating that the P–Tr boundary is at the middle of Bed 10, located about 66 cm above the top of the bioclastic limestones of the Changxing Formation (Fig. 2), consistent with Peng and Tong result46. Besides conodont biostratigraphy, large carbon isotope excursions are useful for stratigraphic correlation 47 13 13 from the end-Permian to the Early-Middle Triassic . Tere are two negative excursions of δ Ccarb and δ Corg across the P–Tr boundary in deep-water sections 26. Two negative δ13C excursions occur at the Meishan section, within Clarkina meishanensis and Isaricella isarcica zones respectively, and are intercalated by a weaker posi- tive shif around the H. parvus zone45 (Fig. 3A). However, due to the major regression at the end-Permian10, 13 the frst negative excursion record disappeared at most shallow-water sections (Fig. 3C). Te δ Ccarb record from Liangfengya contains two negative
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