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Fig. 12 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 12. Representatives of Wuchiapingian ammonoids from the Hambast Formation of Abadeh, Central Iran. A. Pseudogastrioceras abichianum (Möller, 1879), DVGI, no. 10/850 (most likely Clarkina leveni Zone). B. Paraceltitites sp., DVGI, no. 1/850 (most likely Clarkina transcaucasica Zone): right lateral (B1) and ventral (B2) views. C. Paratirolites waageni (Stoyanov, 1910), DVGI no. 11/850 (Hambast Formation, upper Member 7), late Dorashamian Paratirolites kittli Zone.

Fig. 10 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 10. Ammonoids suture lines from lower Olenekian, Mesohedenstroemia bosphorensis Zone; SMID quarry at the Artyom environs, south Primorye. A. Ceratitid Inyoites sedini sp. nov., DVGI 1/851 (holotype). Suture line, height 21.2 mm (A1); whorl cross−section, height 21.1 mm (A2). B. Suture line of phylloceratid Subbalhaeceras shigetai gen. and sp. nov., DVGI 2/851 (holotype). Abbreviations: L, lateral lobe; U, umbilical lobe; V, ventral lobe.

Fig. 7 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 7. Mangyshlak, Kazakhstan: temporal ranges of ammonoid genera of the upper Olenekian. Abbreviation: Reg. Series, Regional Series.

Fig. 1 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 1. Study areas: 1, Iran−Transcaucasia area; 2, Siberia and northern Russian Far East; 3, southern Russian Far East (South Primorye and Amur River); 4, Mangyshlak, Kazakhstan.

Fig. 2 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 2. View of the Permian–Triassic sequences of the section from the Wuchiapingian–Changhsingian Hambast (H) Formation to latest Changhsigian– Induan Elikah (E) Formation at the Hambast region, 28 km to south−western of the village of Abaraku, Abadeh, Central Iran.

Fig. 8 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 8. Suture lines of some Prolecanitida. A. Mesohedenstroemia olgae sp. nov., DVGI 2/851 (holotype), height 18.4 mm; Lower Olenekian, Mesohedenstroemia bosphorensis Zone; SMID quarry at the Artyom environs, south Primorye. B, C. Hedenstroemia tscherskii (Popov, 1961). Lower Olenekian, Lepiskites kolymensis Zone; Kenyelichi River, Kolyma River basin. B. DVGI 256−3b, height 60.0 mm (B1) and 73.0 mm (B2). C. DVGI 255−19c, height 73.0 mm. Abbreviations: D, dorsal lobe; I, inner lateral lobe; L, lateral lobe; U, umbilical lobe; V, ventral lobe.

Fig. 11 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 11. Suggested phylogenetic relationships in the Changhsingian–Olenekian goniatitid, prolecanitid, ceratitid, and phylloceratid ammonoid superfamilies and families.

Fig. 9 in The ammonoid recovery after the end-Permian mass extinction: Evidence from the Iran-Transcaucasia area, Siberia, Primorye, and Kazakhstan

Fig. 9. Some Early Olenekian Prolecanitida, Ceratitida, and Phylloceratida from Lower Olenekian, Mesohedenstroemia bosphorensis Zone; SMID quarry at the Artyom environs, South Primorye. A. Prolecantid Mesohedenstroemia olgae sp. nov., DVGI 2/851 (holotype), right lateral (A1) and ventral (A2) views. B. Ceratitid Inyoites sedini sp. nov., DVGI 1/851 (holotype). C. Phylloceratid Subbalhaeceras shigetai gen. and sp. nov., DVGI 2/851 (holotype), right lateral (C1), left lateral (C2), ventral (C3) views.

Fig. 7 in The fossil record of early tetrapods: Worker effort and the end-Permian mass extinction

Fig. 7. Species discovery curves for several groups of fossil organisms show substantial differences in form. All discovery curves are shown as percentages, even though final totals, in 2003, are very different: trilobites (n = 4126), early tetrapods (n = 515), dinosaurs (n = 694), fossil birds (n = 221), and fossil mammals of North America (n = 3340). The horizontal line marks the "half life" of the discovery curve, the date by which half the currently valid taxa had accumulated. Data from these sources: trilobites (Tarver et al. 2007), dinosaurs (Benton 2008), fossil birds (Fountaine et al. 2008), fossil mammals (Alroy 2002).

Fig. 2 in The fossil record of early tetrapods: Worker effort and the end-Permian mass extinction

Fig. 2. Perceptions of early tetrapod diversity at three points in research time, 1900, 1950, and 2000. Total numbers of valid species are indicated per series; the 1900 data distribution differs significantly from those for 1950 and 2000, but the 1950 and 2000 distributions do not differ significantly (see text).

Fig. 1 in The fossil record of early tetrapods: Worker effort and the end-Permian mass extinction

Fig. 1. Discovery curve of valid early tetrapod species (i.e., tetrapods, excluding Lissamphibia and Amniota), plotted against publication year. Species determined as synonymous or dubious in recent revisions are excluded. The curves show proportions through time, rising to 100% of current knowledge, for all early tetrapods (n = 528) and two major sub−divisions, temnospondyls (n = 368), and lepospondyls (n = 85).

Fig. 6 in The fossil record of early tetrapods: Worker effort and the end-Permian mass extinction

Fig. 6. Cumulative discovery curve of species of early tetrapods showing the relative completeness for each of the eight stratigraphic series, divided into two panels, from Upper Devonian to Middle Permian (A), and Upper Permian to Upper Triassic (B), plotted against decades in research time. The horizontal line marks the "half life" of the discovery curve, the date by which half the currently valid taxa had accumulated. Numbers of taxa per series are: Upper Devonian (17), Lower Carboniferous (25), Upper Carboniferous (108), Lower Permian (125), Middle Permian (36), Upper Permian (20), Lower Triassic (100), Middle Triassic (46), Upper Triassic (5), Jurassic (5), Cretaceous (1).

Fig. 4 in The fossil record of early tetrapods: Worker effort and the end-Permian mass extinction

Fig. 4. Cumulative discovery curves of species of early tetrapods showing the relative completeness for each of the nine major geographic regions: North America, Europe, and Africa (A), South America, Greenland, and Australia (B), Asia, India, and Russia (C), plotted against decades in research time. The horizontal line marks the "half life" of the discovery curve, the date by which half the currently valid taxa had accumulated. Total numbers of taxa are given for each continent.

Fig. 3 in The fossil record of early tetrapods: Worker effort and the end-Permian mass extinction

Fig. 3. Histogram of the total number of valid early tetrapod species from each major geographic region. Totals are: Europe (171), North America (156), Russia (77), Africa (51), Australia (30), India (14), Asia excluding India (12), South America (11), and Greenland (9).

opencc-zeroMay 2020View details →

Data from: Ostracods from the end-Permian mass extinction in the Aras Valley section (Northwest Iran)

The Aras Valley section (NW Iran) exposes a sedimentary succession that allows to study ostracod diversity patterns during/across the end-Permian mass extinction because of its ubiquitous fossil record. For the present study, 59 samples were investigated for their ostracod abundances, which ranged from 4 to 31500 specimens per 500 g. In 45 sample horizons, the ostracods were identified to the species-level. In total, 3,425 specimens were determined and 62 species were identified, of which one genus and ten species are described for the first time: Fabalicypris veronicae Gliwa, sp. nov., Orthobairdia capuliformis Gliwa, sp. nov., Araxobairdia formosa Gliwa, gen. et sp. nov., Bairdiacypris kathleenae Gliwa, sp. nov., Eumiraculum mettei Gliwa, sp. nov., Liuzhinia julfensis Gliwa, sp. nov., Carinaknightina hofmanni Gliwa, sp. nov., Cavellina fosteri Gliwa, sp. nov., Cavellina hairapetiani Gliwa, sp. nov. and Hungaroleberis striatus Forel, sp. nov. The assemblages show, at the end-Permian mass extinction event, a complete turnover from a low-diversity Fabalicypris-dominated pre-extinction community to a more diverse Bairdiacypris-dominated post-extinction community. The turnover coincides with the significant temperature increase that was previously recorded from NW Iranian sections. The low diversity in the horizon immediately below the extinction horizon indicates that environmental changes, such as thermal stress, may have had an impact on the ostracod assemblages prior to the extinction event. In comparison with other diverse ostracod assemblages from the Palaeotethyan realm, the ostracods of the Aras Valley section are not associated with microbialites.

opencc-zeroDec 2021View details →

Data from: Machine learning identifies ecological selectivity patterns across the end-Permian mass extinction

The end-Permian mass extinction occurred alongside a large swathe of environmental changes that are often invoked as extinction mechanisms, even when a direct link is lacking. One way to elucidate the cause(s) of a mass extinction is to investigate extinction selectivity as it can reveal critical information on organismic traits as key determinants of extinction and survival. Here we show that machine learning algorithms, specifically gradient boosted decision trees, can be used to identify determinants of extinction as well as predict extinction risk. To understand which factors led to the end-Permian mass extinction during an extreme global warming event, we quantified the ecological selectivity of marine extinctions in the well-studied South China region. We find that extinction selectivity varies between different groups of organisms and that a synergy of multiple environmental stressors best explains the overall end-Permian extinction selectivity pattern. Extinction risk was greater for genera that had a low species richness, had narrow bathymetric ranges limited to deep-water habitats, had a stationary mode of life, possessed a siliceous skeleton or, less critically, had calcitic skeletons. These selective losses directly link the extinction to the environmental effects of rapid injections of carbon dioxide into the ocean-atmosphere system, specifically the combined effects of expanded oxygen minimum zones, rapid warming, and potentially ocean acidification.

opencc-zeroJun 2022View details →

Data from: Gradual warming prior to the end-Permian mass extinction

The biggest known mass extinction in the history of animal life occurred at the Permian-Triassic boundary and has often been linked to global warming. Previous studies suggested that a geologically rapid (less than 40 kyr) temperature increase of more than 10°C occurred simultaneously with the main extinction pulse. This hypothesis is challenged by geochemical and palaeontological data indicating profound environmental perturbations and a temperature rise prior to the main extinction. Using Secondary Ion Mass Spectrometry (SIMS), we measured oxygen isotope ratios from Changhsingian (Late Permian) ostracods of northwestern Iran. Our data show that ambient seawater temperature began to rise at least 300 kyr prior to the main extinction event. Gradual warming by approximately 12°C was probably responsible for initial environmental degradation that eventually culminated in the global end-Permian mass extinction.

publicJul 2020View details →

Data from: Ostracods from the end-Permian mass extinction in the Aras Valley section (Northwest Iran)

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publicAug 2022View details →

Data from: Gradual warming prior to the end-Permian mass extinction

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