[1] Erwin D H. Extinction: How Life on Earth Nearly Ended 250 Million Years Ago. Princeton, NJ: Princeton University Press, 2006: 320. [2] Knoll A H, Bambach R K, Payne J L, et al. Paleophysiology and end-Permian mass extinction. Earth and Planetary Science Letters, 2007, 256: 295-313. [3] Chen Z Q, Benton M J. The timing and pattern of biotic recovery following the end-Permian mass extinction. Nature Geoscience, 2012, 5: 375-383. [4] Sun Y D, Joachimski M M, Wignall P B, et al. Lethally hot temperatures during the Early Triassic greenhouse. Science, 2012, 338: 366-370. [5] Grasby S E, Beauchamp B, Embry A, et al. Recurrent Early Triassic ocean anoxia. Geology, 2013, 41: 175-178. [6] Huang Y G, Chen Z Q, Wignall P B, et al. Latest Permian to Middle Triassic redox condition variations in ramp settings, South China: Pyrite framboid evidence. Geological Society of America Bulletin, 2017, 129 (1/2): 229-243. [7] Zhang G J, Zhang X L, Hu D P, et al. Redox chemistry changes in the Panthalassic Ocean linked to the end-Permian mass extinction and delayed Early Triassic biotic recovery. Proceedings of the National Academy of Sciences of the United States of America, 2017, 114: 1806-1810. [8] Zhang F F, Algeo T J, Cui Y, et al. Global-ocean redox variations across the Smithian-Spathian boundary linked to concurrent climatic and biotic changes. Earth-Science Reviews, 2019, 195: 147-168. [9] Algeo T J, Twitchett R J. Anomalous Early Triassic sediment fluxes due to elevated weathering rates and their biological consequences. Geology, 2010, 38 (11): 1023-1026. [10] Sun H, Xiao Y L, Gao Y J, et al. Rapid enhancement of chemical weathering recorded by extremely light seawater lithium isotopes at the Permian-Triassic boundary. Proceedings of the National Academy of Sciences of the United States of America, 2018, 115 (15): 3782-3787. [11] Payne J L, Lehrmann D J, Wei J Y, et al. Large perturbations of the carbon cycle during recovery from the end-Permian extinction. Science, 2004, 305: 506-509. [12] Horacek M, Richoz S, Brandner R, et al. Evidence for recurrent changes in Lower Triassic oceanic circulation of the Tethys: The δ13C record from marine sections in Iran. Palaeogeography Palaeoclimatology Palaeoecology, 2007, 252: 355-369. [13] Tong J N, Zuo J X, Chen Z Q. Early Triassic carbon isotope excursions from South China: Proxies for devastation and restoration of marine ecosystems following the end-Permian mass extinction. Geological Journal, 2007, 42: 371-389. [14] Galfetti T, Bucher H, Brayard A, et al. Late Early Triassic climate change: Insights from carbonate carbon isotopes, sedimentary evolution and ammonoid paleobiogeography. Palaeogeography Palaeoclimatology Palaeoecology, 2007, 243: 394-411. [15] Zhang L, Orchard M J, Algeo T J, et al. An intercalibrated Triassic conodont succession and carbonate carbon isotope profile, Kamura, Japan. Palaeogeography Palaeoclimatology Palaeoecology, 2019, 519: 65-83. [16] Tong J N, Yin H F. The Lower Triassic of South China. Journal of Asian Earth Sciences, 2002, 20: 803-815. [17] Zhao L S, Chen Y L, Chen Z Q, et al. Uppermost Permian to Lower Triassic conodont zonation from Three Gorges area, South China. Palaios, 2013, 28: 523-540. [18] Luo M, George A D, Chen Z Q. Sedimentology and ichnology of two Lower Triassic sections in South China: Implications for the biotic recovery following the end-Permian mass extinction. Global and Planetary Change, 2016, 144: 198-212. [19] Hu S X, Zhang Q Y, Chen Z Q, et al. The Luoping biota: Exceptional preservation, and new evidence on the Triassic recovery from end-Permian mass extinction. Proceedings of the Royal Society B, 2011, 278: 2274-2282. [20] Benton M J, Zhang Q Y, Hu S X, et al. Exceptional vertebrate biotas from the Triassic of China, and the expansion of marine ecosystems after the Permo-Triassic mass extinction. Earth-Science Reviews, 2014, 137: 85-128. [21] Kaufman A J, Knoll A H. Neoproterozoic variations in the C-isotopic composition of seawater:Stratigraphic and biogeochemical implications. Precambrian Research, 1995, 73: 27-49. [22] Knauth L P, Kennedy M J. The late Precambrian greening of the Earth. Nature, 2009, 460: 728-732. [23] Derry L A. A burial diagenesis origin for the Ediacaran Shuram-Wonoka carbon isotope anomaly. Earth and Planetary Science Letters, 2010, 294: 152-162. [24] Swart P K. The geochemistry of carbonate diagenesis: The past, present, and future. Sedimentology, 2015, 62: 1233-1304. [25] Higgins J A, Blattler C L, Lundstrom E A, et al. Mineralogy, early marine diagenesis, and the chemistry of shallow-water carbonate sediments. Geochimica et Cosmochimica Acta, 2018, 220: 512-534. [26] Ahm A C, Bjerrum C J, Blattler C L, et al. Quantifying early marine diagenesis in shallow-water carbonate sediments. Geochimica et Cosmochimica Acta, 2018, 236: 140-159. [27] Payne J L, Kump L R. Evidence for recurrent Early Triassic massive volcanism from quantitative interpretation of carbon isotope fluctuations. Earth and Planetary Science Letters, 2007, 256: 264-277. [28] Hammer Ø, Jones M T, Schneebeli-Hermann E, et al. Are Early Triassic extinction events associated with mercury anomalies? A reassessment of the Smithian/Spathian boundary extinction. Earth-Science Reviews, 2019, 195: 179-190. [29] Sexton P F, Norris R D, Wilson P A, et al. Eocene global warming events driven by ventilation of oceanic dissolved organic carbon. Nature, 2001, 471: 349-352. [30] Chen Z Q, Wang Y B, Kershaw S, et al. Early Triassic stromatolites in a siliciclastic nearshore setting in northern Perth Basin, Western Australia: Geobiologic features and implications for post-extinction microbial proliferation. Global and Planetary Change, 2014, 121: 89-100. [31] Fang Y H, Chen Z Q, Kershaw S, et al. An Early Triassic (Smithian) stromatolite associated with giant ooid banks from Lichuan (Hubei Province), South China: Environment and controls on its formation. Palaeogeography Palaeoclimatology Palaeoecology, 2017, 486: 108-122. [32] Zhang G J, Zhang X L, Shen Y. Quantitative constraints on carbon cycling and temporal changes in episodic euxinia during the end-Permian mass extinction in South China. Chemical Geology, 2021, 562: 120036. [33] Zhang G J, Zhang X L, Li D D, et al. Evidence for the expansion of anoxia during the Smithian from a quantitative interpretation of paired C-isotopes. Global and Planetary Change, 2021, 204: 103551. [34] Feng X Q, Chen Z Q, Bottjer D J, et al. Additional records of ichnogenus Rhizocorallium from the Lower and Middle Triassic, South China: Implications for biotic recovery after the end-Permian mass extinction. Geological Society of America Bulletin, 2018, 130: 1197-1215. [35] Luo M, Shi G R, Buatois L A, et al. Trace fossils as proxy for biotic recovery after the end-Permian mass extinction: A critical review. Earth-Science Reviews, 2020, 203: 103059. |