Frequent high-temperature volcanic combustion events delayed biotic recovery after the end-Permian mass extinction

Saito, Ryosuke; Kaiho, Kunio; Tian, Li; Takahashi, Satoshi

doi:10.1016/j.epsl.2023.118194

Cited by 6 publications

(5 citation statements)

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“…The ratio of the sum of benzo[e]pyrene, benzo[ghi]perylene, and coronene to phenanthrene (5- to 7-ring PAH index) is used as an indicator of heating events 9 – 11 , 31 . The 5- to 7-ring PAH index is significantly elevated in heating events and mass extinctions compared to their background values (non-extinction periods) 9 – 11 .…”

Section: Resultsmentioning

confidence: 99%

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Role of volcanism and impact heating in mass extinction climate shifts

Kaiho

2024

Sci Rep

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This study investigates the mechanisms underlying the varied climate changes witnessed during mass extinctions in the Phanerozoic Eon. Climate shifts during mass extinctions have manifested as either predominant global cooling or predominant warming, yet the causes behind these occurrences remain unclear. We emphasize the significance of sedimentary rock temperature in comprehending these climate shifts. Our research reveals that low-temperature heating of sulfide leads to global cooling through the release of sulfur dioxide (SO2), while intermediate-temperature heating of hydrocarbons and carbonates releases substantial carbon dioxide (CO2), contributing to global warming. High-temperature heating additionally generates SO2 from sulfate, further contributing to global cooling. Different degrees of contact heating of the host rock can lead to different dominant volatile gas emissions, crucially driving either warming or cooling. Moreover, medium to high-temperature shock-heating resulting from asteroid impacts produces soot from hydrocarbons, also contributing to global cooling. Large-scale volcanic activity and asteroid impacts are both events that heat rocks, emitting the same gases and particles, causing climate changes. The findings elucidate the critical role of heating temperature and heating time in understanding major climate changes during mass extinctions.

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Section: Resultsmentioning

confidence: 99%

“…It serves as an indicator of heating temperature. Previous studies 9 – 12 , 31 have utilized this index to investigate mass extinction events. The coronene index data are compiled in Table 1 .…”

Section: Methodsmentioning

confidence: 99%

Role of volcanism and impact heating in mass extinction climate shifts

Kaiho

2024

Sci Rep

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“…1 ). The transition marks the loss of more than 200 species across the region, an extinction magnitude of ∼60%, that may have occurred in as little as 1000 years [ 11 ]. Losses were especially severe amongst some shallow-water groups such as calcareous algae, fusulinid foraminifers, gastropods and ammonoids, whilst ostracods and conodonts were little affected at this level [ 7 , 12 , 13 ].…”

Section: Introductionmentioning

confidence: 99%

“…This crisis has long been known as the end-Permian mass extinction and many earlier studies (and even some recent ones [ 8 , 14 ]) considered this phase to mark the end of a prolonged period of diversity decline. In contrast, this crisis is more widely regarded as being geologically rapid, with losses occurring within a few thousand years [ 11 , 15 , 16 ]. The subsequent interval, straddling the Permo-Triassic boundary, is intriguing in that the marine fauna consists of a mixture of Permian survivors and newly originating species [ 9 ].…”

Section: Introductionmentioning

confidence: 99%

The great catastrophe: causes of the Permo-Triassic marine mass extinction

Wignall,

Bond

2023

National Science Review

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The marine losses during the Permo-Triassic mass extinction were the worst ever experienced. All groups were badly affected, especially amongst the benthos (e.g. brachiopods, corals, bryozoans, foraminifers, ostracods). Planktonic populations underwent a fundamental change with eukaryotic algae being replaced by nitrogen-fixing bacteria, green-sulphur bacteria, sulphate-reducing bacteria and prasinophytes. Detailed studies of boundary sections, especially those in South China, have resolved the crisis to a ∼55 kyr interval straddling the Permo-Triassic boundary. Many of the losses occur at the beginning and end of this interval painting a picture of a two-phase extinction. Improved knowledge of the extinction has been supported by numerous geochemical studies that allow diverse proposed extinction mechanisms to be studied. A transition from oxygenated to anoxic-euxinic conditions is seen in most sections globally, although the intensity and timing shows regional variability. Decreased ocean ventilation coincides with rapidly rising temperatures and many extinction scenarios attribute the losses to both anoxia and high temperatures. Other kill mechanisms include ocean acidification for which there is conflicting support from geochemical proxies and, even less likely, siltation (burial under a massive influx of terrigenous sediment) which lacks substantive sedimentological evidence. The ultimate driver of the catastrophic changes at the end of the Permian was likely Siberian Trap eruptions and their associated carbon dioxide emissions with consequences such as warming, ocean stagnation and acidification. Volcanic winter episodes stemming from Siberian volcanism have also been linked to the crisis, but the short-term nature of these episodes (<decades) and the overwhelming evidence for rapid warming during the crisis makes this an unlikely cause. Finally, whilst the extinction is well studied in equatorial latitudes, a different history is found in northern Boreal latitudes including an earlier crisis which merits further study in order to fully understand the course and cause of the Permo-Triassic extinctions.

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“…Palaeoenvironmental reconstructions of the Permian-Triassic interval have primarily focused on the period of time surrounding the PTME (e.g., Wignall and Twitchett, 1996;Lehrmann et al, 2003;Thomas et al, 2004;Algeo et al, 2007;Son et al, 2007;Grasby and Beauchamp, 2009;Bond and Wignall, 2010;Brookfield et al, 2010;Liao et al, 2010;Richoz et al, 2010;Varol et al, 2011). Only a handful of studies have produced continuous environmental records across the entire Lower Triassic interval of environmental instability at the regional or local scale (e.g., Shen et al, 2015;Lau et al, 2016;Grasby et al, 2021;Ishizaki and Shiino, 2023;Saito et al, 2023). Analysis of paleobiologic trends during this period suggests that recovery was often sluggish or reset by persistent environmental stresses (Pietsch et al, 2014;Song et al, 2014;Woods et al, 2019), resulting in a slow biotic rebound that frequently stretched well beyond the earliest Triassic, to perhaps as late as the early middle Triassic (Anisian) (e.g., Schubert, 1989;Hallam, 1991;Twitchett and Wignall, 1996;Boyer et al, 2004;Pruss and Bottjer, 2004;Twitchett and Barras, 2004;Nützel and Schulbert, 2005;Baucon and De Carvalho, 2016;Golding, 2021;Wang et al, 2022;Zhu et al, 2022).…”

Section: Introductionmentioning

confidence: 99%

Hyperthermal-driven anoxia and reduced productivity in the aftermath of the Permian-Triassic mass extinction: a case study from Western Canada

Woods,

Zonneveld,

Wakefield

2023

Front. Earth Sci.

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Introduction: The eruption of the Siberian Traps near the Permian-Triassic boundary (PTB) resulted in the rapid input of vast amounts of CO2 into the atmosphere and the subsequent development of a hothouse climate across much of the Early Triassic. The distribution of environmental stresses led to a complex recovery as survivors navigated high SSTs in shallow settings and an expanded OMZ that impinged upon the continental shelves. The Ursula Creek section of western British Columbia preserves a complete Lower-lowermost Middle Triassic sedimentary record of deep-water facies and provides a means to examine how offshore oceanic conditions varied along the western continental margin of Pangaea across the PTB and the entire Permian-Triassic recovery interval.Methods: A total of 204 samples were collected from the uppermost Permian Fantasque Formation, the Griesbachian—Dienerian Grayling Formation and the Smithian—Anisian Toad Formation and analyzed for major, minor, and trace elements in addition to %TOC contents.Results: Anoxic to euxinic conditions were persistent during deposition of most of the study interval based on lithologic indicators (finely-laminated siltstone that lacks trace fossils and a benthic fauna) and elevated Mo, U, and V enrichment factors (EFs). Ba, Cu, Ni, P, and Zn EFs indicate dampened productivity (EFs <1) across the much of the Early Triassic that was the result of weakened upwelling during a global hothouse interval. An increase in Cu, Ni, P, and Zn enrichment factors during the Anisian track a decline in global temperatures and the reestablishment of coastal upwelling as global thermal gradients and wind speeds increased.Discussion: The results of this study point to the persistence of hyperthermal events and associated environmental stressors and underscores the urgency of curbing modern greenhouse gas emissions to prevent Earth from tipping into a hothouse state.

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Frequent high-temperature volcanic combustion events delayed biotic recovery after the end-Permian mass extinction

Cited by 6 publications

References 67 publications

Role of volcanism and impact heating in mass extinction climate shifts

Role of volcanism and impact heating in mass extinction climate shifts

The great catastrophe: causes of the Permo-Triassic marine mass extinction

Hyperthermal-driven anoxia and reduced productivity in the aftermath of the Permian-Triassic mass extinction: a case study from Western Canada

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