Earth:Toarcian Oceanic Anoxic Event

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Short description: Anoxic event in the Jurassic period

The Toarcian extinction event, also called the Pliensbachian-Toarcian extinction event,[1][2] the Early Toarcian mass extinction,[3] the Early Toarcian palaeoenvironmental crisis,[4] or the Jenkyns Event,[5][6][7] was an extinction event that occurred during the early part of the Toarcian age, approximately 183 million years ago, during the Early Jurassic. The extinction event had two main pulses,[4] the first being the Pliensbachian-Toarcian boundary event (PTo-E).[8] The second, larger pulse, the Toarcian Oceanic Anoxic Event (TOAE), was a global oceanic anoxic event,[9] representing possibly the most extreme case of widespread ocean deoxygenation in the entire Phanerozoic eon.[10] In addition to the PTo-E and TOAE, there were multiple other, smaller extinction pulses within this span of time.[8]

Occurring during the supergreenhouse climate of the Early Toarcian Thermal Maximum (ETTM),[11] the Early Toarcian extinction was associated with large igneous province volcanism,[12] which elevated global temperatures,[11] acidified the oceans,[13] and prompted the development of anoxia,[14] leading to severe biodiversity loss.[15] The biogeochemical crisis is documented by a high amplitude negative carbon isotope excursions,[16][17] as well as black shale deposition.[18]

Timing

The Early Toarcian extinction event occurred in two distinct pulses,[4] with the first event being classified by some authors as its own event unrelated to the more extreme second event.[19] The first, more recently identified pulse occurred during the mirabile subzone of the tenuicostatum ammonite zone, coinciding with a slight drop in oxygen concentrations and the beginning of warming following a late Pliensbachian cool period.[20] This first pulse, occurring near the Pliensbachian-Toarcian boundary,[21] is referred to as the PTo-E.[8][9] The TOAE itself occurred near the tenuicostatum–serpentinum ammonite biozonal boundary,[22] specifically in the elegantulum subzone of the serpentinum ammonite zone, during a marked, pronounced warming interval.[20] The TOAE lasted for approximately 500,000 years,[23][24][25] though a range of estimates from 200,000 to 1,000,000 years have also been given.[26] The PTo-E primarily affected shallow water biota, while the TOAE was the more severe event for organisms living in deep water.[27]

Causes

Geological, isotopic, and palaeobotanical evidence suggests the late Pliensbachian was an icehouse period.[28][29][30] These ice sheets are believed to have been thin and stretched into lower latitudes, making them extremely sensitive to temperature changes.[31] A warming trend lasting from the latest Pliensbachian to the earliest Toarcian was interrupted by a "cold snap" in the middle polymorphum zone, equivalent to the tenuicostatum ammonite zone, which was then followed by the abrupt warming interval associated with the TOAE.[32] This global warming, driven by rising atmospheric carbon dioxide, was the mainspring of the early Toarcian environmental crisis.[3] Carbon dioxide levels rose from about 500 ppm to about 1,000 ppm.[33] Seawater warmed by anywhere between 3 °C and 7 °C, depending on latitude.[34] At the height of this supergreenhouse interval, global sea surface temperatures (SSTs) averaged about 21 °C.[3]

The eruption of the Karoo-Ferrar Large Igneous Province is generally attributed to have caused the surge in atmospheric carbon dioxide levels.[12][6][35] Argon-argon dating of Karoo-Ferrar rhyolites points to a link between Karoo-Ferrar volcanism and the extinction event,[36] a conclusion reinforced by uranium-lead dating[37][38][39] and palaeomagnetism.[40] The values of 187Os/188Os rose from ~0.40 to ~0.53 during the PTo-E and from ~0.42 to ~0.68 during the TOAE, and many scholars conclude this change in osmium isotope ratios evidences the responsibility of this large igneous province for the biotic crises.[41] Mercury anomalies from the approximate time intervals corresponding to the PTo-E and TOAE have likewise been invoked as tell-tale evidence of the ecological calamity's cause being a large igneous province,[42][43][44] although some researchers attribute these elevated mercury levels to increased terrigenous flux.[45] There is evidence that the motion of the African Plate suddenly changed in velocity, shifting from mostly northward movement to southward movement. Such shifts in plate motion are associated with similar large igneous provinces emplaced in other time intervals.[46] A 2019 geochronological study found that the emplacement of the Karoo-Ferrar large igneous province and the TOAE were not causally linked, and simply happened to occur rather close in time, contradicting mainstream interpretations of the TOAE. The authors of the study conclude that the timeline of the TOAE does not match up with the course of activity of the Karoo-Ferrar magmatic event.[47]

The large igneous province also intruded into coal seams, releasing even more carbon dioxide and methane than it otherwise would have.[48][16] Magmatic sills are also known to have intruded into shales rich in organic carbon, causing additional venting of carbon dioxide into the atmosphere.[49]

In addition, possible associated release of deep sea methane clathrates has been potentially implicated as yet another cause of global warming.[50][51][52] Episodic melting of methane clathrates dictated by Milankovitch cycles has been put forward as an explanation fitting the observed shifts in the carbon isotope record.[53][26][54] Other studies contradict and reject the methane hydrate hypothesis, however, concluding that the isotopic record is too incomplete to conclusively attribute the isotopic excursion to methane hydrate dissociation,[55] that carbon isotope ratios in belemnites and bulk carbonates are incongruent with the isotopic signature expected from a massive release of methane clathrates,[56] that much of the methane released from ocean sediments was rapidly sequestered, buffering its ability to act as a major positive feedback,[57] and that methane clathrate dissociation occurred too late to have had an appreciable causal impact on the extinction event.[58] Hypothetical release of methane clathrates extremely depleted in heavy carbon isotopes has furthermore been considered unnecessary as an explanation for the carbon cycle disruption.[59]

It has also been hypothesised that the release of cryospheric methane trapped in permafrost amplified the warming and its detrimental effects on marine life.[60][61] Obliquity-paced carbon isotope excursions have been interpreted as some researchers as reflective of permafrost decline and consequent greenhouse gas release.[62]

Geochemical evidence from what was then the northwestern European epicontinental sea suggests that a shift from cooler, more saline water conditions to warmer, fresher conditions prompted the development of significant density stratification of the water column and induced anoxia.[24] Rising seawater temperatures amidst a transition from icehouse to greenhouse conditions retarded ocean circulation, aiding the establishment of anoxic conditions.[63] Further consequences resulting from large igneous province activity included increased silicate weathering and an acceleration of the hydrological cycle,[64][65] as shown by a increased amount of terrestrially derived organic matter found in sedimentary rocks of marine origin during the TOAE.[66][67] A -0.5% excursion in δ44/40Ca provides further evidence of increased continental weathering.[68] The enhanced continental weathering in turn led to increased eutrophication that helped drive the anoxic event in the oceans.[14][69] Continual transport of continentally weathered nutrients into the ocean enabled high levels of primary productivity to be maintained over the course of the TOAE.[24] Organic plant matter also entered the marine realm as rising sea levels inundated low-lying lands and transported vegetation outwards into the ocean.[70] An alternate model for the development of anoxia is that epicontinental seaways became salinity stratified with strong haloclines, chemoclines, and thermoclines. This caused mineralised carbon on the seafloor to be recycled back into the photic zone, driving widespread primary productivity and in turn anoxia.[71] The freshening of the Arctic Ocean by way of melting of Northern Hemisphere ice caps was a likely trigger of such stratification and a slowdown of global thermohaline circulation.[72] Stratification also occurred due to the freshening of surface water caused by an enhanced water cycle.[73][74] Extensive organic carbon burial induced by anoxia was a negative feedback loop retarding the otherwise pronounced warming and may have caused global cooling in the aftermath of the TOAE.[75] In anoxic and euxinic marine basins in Europe, organic carbon burial rates increased by ~500%.[5] Furthermore, anoxia was not limited to oceans; large lakes also experienced oxygen depletion and black shale deposition.[76][77]

Euxinia occurred in the northwestern Tethys Ocean during the TOAE, evidenced by enhanced pyrite burial in Zázrivá, Slovakia,[78] enhanced molybdenum burial totalling about 41 Gt of molybdenum,[79] and δ98/95Mo excursions observed in sites in the Cleveland, West Netherlands, and South German Basins.[80] Valdorbia, a site in the Umbria-Marche Apennines, also exhibited euxinia during the anoxic event.[26] There is less evidence of euxinia outside the northwestern Tethys, and it likely only occurred transiently in basins in Panthalassa and the southwestern Tethys.[81] Due to the clockwise circulation of the oceanic gyre in the western Tethys and the rough, uneven bathymetry in the northward limb of this gyre, oxic bottom waters had relatively few impediments to diffuse into the southwestern Tethys, which spared it from the far greater prevalence of anoxia and euxinia that characterised the northern Tethys.[82] The Panthalassan deep water site of Sakahogi was mainly anoxic-ferruginous across the interval spanning the late Pliensbachian to the TOAE, but transient sulphidic conditions did occur during the PTo-E and TOAE.[83] In northeastern Panthalassa, in what is now British Columbia, euxinia dominated anoxic bottom waters.[84]

The early stages of the TOAE were accompanied by a decrease in the acidity of seawater following a substantial decrease prior to the TOAE. Seawater pH then dropped close to the middle of the event, strongly acidifying the oceans.[13] The sudden decline of carbonate production during the TOAE is widely believed to be the result of this abrupt episode of ocean acidification.[85][86][87] Additionally, the enhanced recycling of phosphorus back into seawater as a result of high temperatures and low seawater pH inhibited its mineralisation into apatite, helping contribute to oceanic anoxia. The abundance of phosphorus in marine environments created a positive feedback loop whose consequence was the further exacerbation of eutrophication and anoxia.[88]

The extreme and rapid global warming at the start of the Toarcian promoted intensification of tropical storms across the globe.[89][90]

Effects on biogeochemical cycles

Carbon cycle

Occurring during a broader, gradual positive carbon isotope excursion as measured by δ13C values, the TOAE is associated with a global negative δ13C excursion recognised in fossil wood, organic carbon, and carbonate carbon in the tenuicostatum ammonite zone of northwestern Europe.[91][16] The global ubiquity of this negative δ13C excursion has been called into question, however, due to its absence in certain deposits from the time, such as the Bächental bituminous marls,[92] though its occurrence in areas like Greece has been cited as evidence of its global nature.[93] The negative δ13C shift is also known from the Arabian Peninsula,[94] the Ordos Basin,[95] and the Neuquén Basin.[96] The negative δ13C excursion has been found to be up to -8% in bulk organic and carbonate carbon, although analysis of compound specific biomarkers suggests a global value of around -3% to -4%. In addition, numerous smaller scale carbon isotope excursions are globally recorded on the falling limb of the larger negative δ13C excursion.[16] A positive δ13C excursion, likely resulting from the mass burial of organic carbon during the anoxic event, is known from the subsequent falciferum ammonite zone.[97] The Karoo-Ferrar magmatism released so much carbon dioxide that it disrupted the imprint of the 9 Myr long-term carbon cycle that was otherwise steady and stable during the Jurassic and Early Cretaceous.[98]

Sulphur cycle

A positive sulphur isotope excursion in carbonate-associated sulphate occurs synchronously with the positive carbon isotope excursion in carbonate carbon during the falciferum ammonite zone. This positive sulphur isotope excursion has been attributed to the depletion of isotopically light sulphur in the marine sulphate reservoir that resulted from microbial sulphur reduction in anoxic waters.[99] Similar positive sulphur isotope excursions corresponding to the onset of TOAE are known from pyrites in the Sakahogi and Sakuraguchi-dani localities in Japan, with the Sakahogi site displaying a less extreme but still significant pyritic positive sulphur isotope excursion during the PTo-E.[100]

Effects on life

Marine invertebrates

The extinction event associated with the TOAE primarily affected marine life as a result the collapse of the carbonate factory.[101] Brachiopods were particularly severely hit,[102][2][103] with the TOAE representing one of the most dire crises in their evolutionary history.[104] Brachiopod taxa of large size declined significantly in abundance.[105] Uniquely, the brachiopod genus Soaresirhynchia thrived during the later stages of the TOAE due to its low metabolic rate and slow rate of growth, making it a disaster taxon.[106] The species S. bouchardi is known to have been a pioneer species that colonised areas denuded of brachiopods in the northwestern Tethyan region.[107] Ostracods also suffered a major diversity loss,[108][109] with almost all ostracod clades’ distributions during the time interval corresponding to the serpentinum zone shifting towards higher latitudes to escape intolerably hot conditions near the Equator.[20] Bivalves likewise experienced a significant turnover.[109] The decline of bivalves exhibiting high endemism with narrow geographic ranges was particularly severe.[1] At Ya Ha Tinda, a replacement of the pre-TOAE bivalve assemblage by a smaller, post-TOAE assemblage occurred,[110] while in the Cleveland Basin, the inoceramid Pseudomytiloides dubius experienced the Lilliput effect.[111] Ammonoids, having already experienced a major morphological bottleneck thanks to the Gibbosus Event,[112] about a million years before the Toarcian extinction, suffered further losses in the Early Toarcian diversity collapse.[113] Belemnite richness in the northwestern Tethys dropped during the PTo-E but slightly increased across the TOAE.[114] Belemnites underwent a major change in habitat preference from cold, deep waters to warm, shallow waters.[10] Their average rostrum size also increased, though this trend heavily varied depending on the lineage of belemnites.[114] The Toarcian extinction was unbelievably catastrophic for corals; 90.9% of all Tethyan coral species and 49% of all genera were wiped out.[115] Calcareous nannoplankton that lived in the deep photic zone suffered, with the decrease in abundance of the taxon Mitrolithus jansae used as an indicator of shoaling of the oxygen minimum zone in the Tethys and the Hispanic Corridor.[116] Other affected invertebrate groups included echinoderms,[117] radiolarians,[118] dinoflagellates,[117] and foraminifera.[119][120][108] Trace fossils, an indicator of bioturbation and ecological diversity, became highly undiverse following the TOAE.[121]

Carbonate platforms collapsed during both the PTo-E and the TOAE. Enhanced continental weathering and nutrient runoff was the dominant driver of carbonate platform decline in the PTo-E, while the biggest culprits during the TOAE were heightened storm activity and a decrease in the pH of seawater.[27]

The recovery from the mass extinction among benthos commenced with the recolonisation of barren locales by opportunistic pioneer taxa. Benthic recovery was slow and sluggish, being regularly set back thanks to recurrent episodes of oxygen depletion, which continued for hundreds of thousands of years after the main extinction interval.[122] Many marine invertebrate taxa found in South America migrated through the Hispanic Corridor into European seas after the extinction event, aided in their dispersal by higher sea levels.[123]

Marine vertebrates

The TOAE had minor effects on marine reptiles, in stark contrast to the major impact it had on many clades of marine invertebrates. In fact, in the Southwest German Basin, ichthyosaur diversity was higher after the extinction interval, although this may be in part a sampling artefact resulting from a sparse Pliensbachian marine vertebrate fossil record.[124]

Terrestrial vertebrates

The TOAE is suggested to have caused the extinction of various clades of dinosaurs, including coelophysids, dilophosaurids, and many basal sauropodomorph clades, as a consequence of the remodelling of terrestrial ecosystems caused by global climate change.[15] Some heterodontosaurids and thyreophorans also perished in the extinction event.[125] In the wake of the extinction event, many derived clades of ornithischians, sauropods, and theropods emerged, with most of these post-extinction clades greatly increasing in size relative to dinosaurs before the TOAE.[15] Eusauropods were propelled to ecological dominance after their survival of the Toarcian cataclysm.[126]

Terrestrial plants

The volcanogenic extinction event initially impacted terrestrial ecosystems more severely than marine ones. A shift towards a low diversity assemblage of cheirolepid conifers, cycads, and Cerebropollenites-producers adapted for high aridity from a higher diversity ecological assemblage of lycophytes, conifers, seed ferns, and wet-adapted ferns is observed in the palaeobotanical and palynological record over the course of the TOAE.[69] The coincidence of the zenith of Classopolis and the decline of seed ferns and spore producing plants with increased mercury loading implicates heavy metal poisoning as a key contributor to the floristic crisis during the Toarcian mass extinction.[127] Poisoning by mercury, along with chromium, copper, cadmium, arsenic, and lead is speculated to be responsible for heightened rates of spore malformation and dwarfism concomitant with enrichments in all these toxic metals.[128]

Geologic effects

The TOAE was associated with widespread phosphatisation of marine fossils believed to result from the warming-induced increase in weathering that increased phosphate flux into the ocean. This produced exquisitely preserved lagerstätten across the world, such as Ya Ha Tinda, Strawberry Bank, and the Posidonia Shale.[129]

As is common during anoxic events, black shale deposition was widespread during the deoxygenation events of the Toarcian.[130][18][131] Toarcian anoxia was responsible for the deposition of commercially extracted oil shales,[132] particularly in China.[133][134]

Enhanced hydrological cycling caused clastic sedimentation to accelerate during the TOAE; the increase in clastic sedimentation was synchronous with excursions in 187Os/188Os, 87Sr/86Sr, and δ44/40Ca.[135]

Additionally, the Toarcian was punctuated by intervals of extensive kaolinite enrichment. These kaolinites correspond to negative oxygen isotope excursions and high Mg/Ca ratios and are thus reflective of climatic warming events that characterised much of the Toarcian.[136] Likewise, illitic/smectitic clays were also common during this hyperthermal perturbation.[137]

Palaeogeographic changes

The intertropical convergence zone migrated southwards across southern Gondwana, turning much of the region more arid. This aridification was interrupted, however, in the spinatus ammonite biozone and across the Pliensbachian-Toarcian boundary itself.[44]

The large rise in sea levels resulting from the intense global warming led to the formation of the Laurasian Seaway, which enabled the flow of cool water low in salt content to flow into the Tethys Ocean from the Arctic Ocean. The opening of this seaway may have potentially acted as a mitigating factor that ameliorated to a degree the oppressively anoxic conditions that were widespread across much of the Tethys.[138]

The enhanced hydrological cycle during early Toarcian warming caused lakes to grow in size.[95] During the anoxic event, the Sichuan Basin was transformed into a giant lake,[139][140] which was believed to be approximately thrice as large as modern-day Lake Superior.[141] Lacustrine sediments deposited as a result of this lake's existence are represented by the Da’anzhai Member of the Ziliujing Formation.[142] Roughly ~460 gigatons (Gt) of organic carbon and ~1,200 Gt of inorganic carbon were likely sequestered by this lake over the course of the TOAE.[141]

Comparison with present global warming

The TOAE and the Palaeocene-Eocene Thermal Maximum have been proposed as analogues to modern anthropogenic global warming based on the comparable quantity of greenhouse gases released into the atmosphere in all three events.[51] Some researchers argue that evidence for a major increase in Tethyan tropical cyclone intensity during the TOAE suggests that a similar increase in magnitude of tropical storms is bound to occur as a consequence of present climate change.[90]

See also

References

  1. ↑ 1.0 1.1 Aberhan, M.; Fürsich, Franz T. (January 2000). "Mass origination versus mass extinction: the biological contribution to the Pliensbachian–Toarcian extinction event". Journal of the Geological Society 157 (1): 55–60. doi:10.1144/jgs.157.1.55. Bibcode: 2000JGSoc.157...55A. https://www.lyellcollection.org/doi/abs/10.1144/jgs.157.1.55. Retrieved 14 May 2023. 
  2. ↑ 2.0 2.1 Caruthers, Andrew H.; Smith, Paul L.; Gröcke, Darren R. (September 2013). "The Pliensbachian–Toarcian (Early Jurassic) extinction, a global multi-phased event" (in en). Palaeogeography, Palaeoclimatology, Palaeoecology 386: 104–118. doi:10.1016/j.palaeo.2013.05.010. Bibcode: 2013PPP...386..104C. https://linkinghub.elsevier.com/retrieve/pii/S0031018213002344. 
  3. ↑ 3.0 3.1 3.2 Gómez, Juan J.; Comas-Rengifo, María J.; Goy, Antonio (20 May 2016). "Palaeoclimatic oscillations in the Pliensbachian (Early Jurassic) of the Asturian Basin (Northern Spain)". Climate of the Past 12 (5): 1199–1214. doi:10.5194/cp-12-1199-2016. Bibcode: 2016CliPa..12.1199G. https://cp.copernicus.org/articles/12/1199/2016/. Retrieved 14 May 2023. 
  4. ↑ 4.0 4.1 4.2 Suan, Guillaume; Mattioli, Emanuela; Pittet, Bernard; Mailliot, Samuel; Lécuyer, Christophe (17 January 2008). "Evidence for major environmental perturbation prior to and during the Toarcian (Early Jurassic) oceanic anoxic event from the Lusitanian Basin, Portugal". Paleoceanography and Paleoclimatology 23 (1): 1–14. doi:10.1029/2007PA001459. Bibcode: 2008PalOc..23.1202S. 
  5. ↑ 5.0 5.1 Kemp, David B.; Suan, Guillaume; Fantasia, Alicia; Jin, Simin; Chen, Wenhan (August 2022). "Global organic carbon burial during the Toarcian oceanic anoxic event: Patterns and controls". Earth-Science Reviews 231: 104086. doi:10.1016/j.earscirev.2022.104086. Bibcode: 2022ESRv..23104086K. https://www.sciencedirect.com/science/article/abs/pii/S0012825222001702. Retrieved 3 January 2023. 
  6. ↑ 6.0 6.1 Reolid, Matías; Mattioli, Emanuela; Duarte, Luís V.; Ruebsam, Wolfgang (2021-09-22). "The Toarcian Oceanic Anoxic Event: where do we stand?" (in en). Geological Society, London, Special Publications 514 (1): 1–11. doi:10.1144/SP514-2021-74. ISSN 0305-8719. Bibcode: 2021GSLSP.514....1R. https://sp.lyellcollection.org/content/early/2021/09/21/SP514-2021-74. 
  7. ↑ Reolid, Matias; Mattioli, Emanuela; Duarte, Luis V.; Marok, Abbas (1 June 2020). "The Toarcian Oceanic Anoxic Event and the Jenkyns Event (IGCP-655 final report)" (in en). Episodes 43 (2): 833–844. doi:10.18814/epiiugs/2020/020051. ISSN 0705-3797. http://www.episodes.org/journal/view.html?doi=10.18814/epiiugs/2020/020051. Retrieved 26 November 2023. 
  8. ↑ 8.0 8.1 8.2 Krencker, F. N.; Bodin, S.; Hoffmann, R.; Suan, Guillaume; Mattioli, E.; Kabiri, L.; Föllmi, K. B.; Immenhauser, A. (June 2014). "The middle Toarcian cold snap: Trigger of mass extinction and carbonate factory demise". Global and Planetary Change 117: 64–78. doi:10.1016/j.gloplacha.2014.03.008. Bibcode: 2014GPC...117...64K. https://www.sciencedirect.com/science/article/abs/pii/S0921818114000629. Retrieved 20 January 2023. 
  9. ↑ 9.0 9.1 Kemp, David B.; Chen, Wenhan; Cho, Tenichi; Algeo, Thomas J.; Shen, Jun; Ikeda, Masayuki (May 2022). "Deep-ocean anoxia across the Pliensbachian-Toarcian boundary and the Toarcian Oceanic Anoxic Event in the Panthalassic Ocean". Global and Planetary Change 212: 103782. doi:10.1016/j.gloplacha.2022.103782. Bibcode: 2022GPC...21203782K. https://www.sciencedirect.com/science/article/abs/pii/S0921818122000492. Retrieved 1 January 2023. 
  10. ↑ 10.0 10.1 Ullmann, Clemens Vinzenz; Thibault, Nicolas; Ruhl, Micha; Hesselbo, Stephen P.; Korte, Christoph (30 June 2014). "Effect of a Jurassic oceanic anoxic event on belemnite ecology and evolution". Proceedings of the National Academy of Sciences of the United States of America 111 (28): 10073–10076. doi:10.1073/pnas.1320156111. PMID 24982187. 
  11. ↑ 11.0 11.1 Scotese, Christopher R.; Song, Haijun; Mills, Benjamin J.W.; van der Meer, Douwe G. (April 2021). "Phanerozoic paleotemperatures: The earth's changing climate during the last 540 million years". Earth-Science Reviews 215: 103503. doi:10.1016/j.earscirev.2021.103503. ISSN 0012-8252. Bibcode: 2021ESRv..21503503S. https://www.researchgate.net/publication/348351275. Retrieved 17 July 2023.  Alt URL
  12. ↑ 12.0 12.1 Pálfy, József; Smith, Paul L. (1 August 2000). "Synchrony between Early Jurassic extinction, oceanic anoxic event, and the Karoo-Ferrar flood basalt volcanism". Geology 28 (8): 747–750. doi:10.1130/0091-7613(2000)28<747:SBEJEO>2.0.CO;2. Bibcode: 2000Geo....28..747P. https://pubs.geoscienceworld.org/gsa/geology/article-abstract/28/8/747/191908/Synchrony-between-Early-Jurassic-extinction. Retrieved 17 April 2023. 
  13. ↑ 13.0 13.1 Müller, Tamás; Jurikova, Hana; Gutjahr, Marcus; Tomašových, Adam; Schlögl, Jan; Liebetrau, Volker; Duarte, Luís v.; Milovský, Rastislav et al. (2020-12-01). "Ocean acidification during the early Toarcian extinction event: Evidence from boron isotopes in brachiopods" (in en). Geology 48 (12): 1184–1188. doi:10.1130/G47781.1. ISSN 0091-7613. Bibcode: 2020Geo....48.1184M. 
  14. ↑ 14.0 14.1 Xia, Guoqing; Mansour, Ahmed (1 October 2022). "Paleoenvironmental changes during the early Toarcian Oceanic Anoxic Event: Insights into organic carbon distribution and controlling mechanisms in the eastern Tethys". Journal of Asian Earth Sciences 237: 105344. doi:10.1016/j.jseaes.2022.105344. Bibcode: 2022JAESc.23705344X. https://www.sciencedirect.com/science/article/abs/pii/S1367912022002759. Retrieved 8 January 2023. 
  15. ↑ 15.0 15.1 15.2 Reolid, M.; Ruebsam, W.; Benton, Michael James (November 2022). "Impact of the Jenkyns Event (early Toarcian) on dinosaurs: Comparison with the Triassic/Jurassic transition". Earth-Science Reviews 234: 104196. doi:10.1016/j.earscirev.2022.104196. Bibcode: 2022ESRv..23404196R. 
  16. ↑ 16.0 16.1 16.2 16.3 Them, T.R.; Gill, B.C.; Caruthers, A.H.; Gröcke, D.R.; Tulsky, E.T.; Martindale, R.C.; Poulton, T.P.; Smith, P.L. (February 2017). "High-resolution carbon isotope records of the Toarcian Oceanic Anoxic Event (Early Jurassic) from North America and implications for the global drivers of the Toarcian carbon cycle" (in en). Earth and Planetary Science Letters 459: 118–126. doi:10.1016/j.epsl.2016.11.021. Bibcode: 2017E&PSL.459..118T. 
  17. ↑ Ros-Franch, Sonia; Echevarría, Javier; Damborenea, Susana E.; Manceñido, Miguel O.; Jenkyns, Hugh C.; Al-Suwaidi, Aisha; Hesselbo, Stephen P.; Riccardi, Alberto C. (1 July 2019). "Population response during an Oceanic Anoxic Event: The case of Posidonotis (Bivalvia) from the Lower Jurassic of the Neuquén Basin, Argentina". Palaeogeography, Palaeoclimatology, Palaeoecology 525: 57–67. doi:10.1016/j.palaeo.2019.04.009. Bibcode: 2019PPP...525...57R. https://www.sciencedirect.com/science/article/abs/pii/S0031018219301415. Retrieved 23 November 2022. 
  18. ↑ 18.0 18.1 Suan, Guillaume; Rulleau, Louis; Mattioli, Emanuela; Suchéras-Marx, Baptiste; Rouselle, Bruno; Pittet, Bernard; Vincent, Peggy; Martin, Jeremy E. et al. (7 February 2013). "Palaeoenvironmental significance of Toarcian black shales and event deposits from southern Beaujolais, France". Geological Magazine 150 (4): 728–742. doi:10.1017/S0016756812000970. Bibcode: 2013GeoM..150..728S. https://www.cambridge.org/core/journals/geological-magazine/article/abs/palaeoenvironmental-significance-of-toarcian-black-shales-and-event-deposits-from-southern-beaujolais-france/790F9CA08A69DE03518736FDE7F5C9BB. Retrieved 13 March 2023. 
  19. ↑ Cecca, Fabrizio; Macchioni, Francesco (2 January 2007). "The two Early Toarcian (Early Jurassic) extinction events in ammonoids". Lethaia 37 (1): 35–56. doi:10.1080/00241160310008257. https://onlinelibrary.wiley.com/doi/abs/10.1080/00241160310008257. Retrieved 14 June 2023. 
  20. ↑ 20.0 20.1 20.2 Arias, Carmen (1 October 2013). "The early Toarcian (early Jurassic) ostracod extinction events in the Iberian Range: The effect of temperature changes and prolonged exposure to low dissolved oxygen concentrations". Palaeogeography, Palaeoclimatology, Palaeoecology 387: 40–55. doi:10.1016/j.palaeo.2013.07.004. Bibcode: 2013PPP...387...40A. https://www.sciencedirect.com/science/article/abs/pii/S0031018213003258. Retrieved 23 November 2022. 
  21. ↑ Littler, Kate; Hesselbo, Stephen P.; Jenkyns, Hugh C. (5 October 2009). "A carbon-isotope perturbation at the Pliensbachian–Toarcian boundary: evidence from the Lias Group, NE England". Geological Magazine 147 (2): 181–192. doi:10.1017/S0016756809990458. https://www.cambridge.org/core/journals/geological-magazine/article/abs/carbonisotope-perturbation-at-the-pliensbachiantoarcian-boundary-evidence-from-the-lias-group-ne-england/FC4BF10D9141FC91B7480399942A6EED. Retrieved 5 August 2023. 
  22. ↑ Al-Suwaidi, Aisha H.; Ruhl, Micha; Jenkyns, Hugh C.; Damborenea, Susana E.; Manceñido, Miguel O.; Condon, Daniel J.; Angelozzi, Gladys N.; Kamo, Sandra L. et al. (23 March 2022). "New age constraints on the Lower Jurassic Pliensbachian–Toarcian Boundary at Chacay Melehue (Neuquén Basin, Argentina)". Scientific Reports 12 (1): 4975. doi:10.1038/s41598-022-07886-x. PMID 35322043. Bibcode: 2022NatSR..12.4975A. 
  23. ↑ Boulila, Slah; Galbrun, Bruno; Sadki, Driss; Gardin, Silvia; Bartolini, Annachiara (1 April 2019). "Constraints on the duration of the early Toarcian T-OAE and evidence for carbon-reservoir change from the High Atlas (Morocco)". Global and Planetary Change 175: 113–128. doi:10.1016/j.gloplacha.2019.02.005. ISSN 0921-8181. https://www.sciencedirect.com/science/article/pii/S092181811830403X. Retrieved 26 November 2023. 
  24. ↑ 24.0 24.1 24.2 Bailey, T. M.; Rosenthal, Y.; McArthur, J. M.; Van de Schootbrugge, B.; Thirlwall, M. F. (25 July 2003). "Paleoceanographic changes of the Late Pliensbachian–Early Toarcian interval: a possible link to the genesis of an Oceanic Anoxic Event". Earth and Planetary Science Letters 212 (3–4): 307–320. doi:10.1016/S0012-821X(03)00278-4. Bibcode: 2003E&PSL.212..307B. https://www.sciencedirect.com/science/article/abs/pii/S0012821X03002784. Retrieved 7 January 2023. 
  25. ↑ McArthur, J. M.; Donovan, D. T.; Thirlwall, M. F.; Fouke, B. W.; Mattey, D. (30 June 2000). "Strontium isotope profile of the early Toarcian (Jurassic) oceanic anoxic event, the duration of ammonite biozones, and belemnite palaeotemperatures". Earth and Planetary Science Letters 179 (2): 269–285. doi:10.1016/S0012-821X(00)00111-4. https://www.sciencedirect.com/science/article/abs/pii/S0012821X00001114. Retrieved 5 August 2023. 
  26. ↑ 26.0 26.1 26.2 Sabatino, Nadia; Neri, Rodolfo; Bellanca, Adriana; Jenkyns, Hugh C.; Baudin, François; Parisi, Guido; Masetti, Daniele (13 July 2009). "Carbon-isotope records of the Early Jurassic (Toarcian) oceanic anoxic event from the Valdorbia (Umbria–Marche Apennines) and Monte Mangart (Julian Alps) sections: palaeoceanographic and stratigraphic implications". Sedimentology 56 (5): 1307–1328. doi:10.1111/j.1365-3091.2008.01035.x. Bibcode: 2009Sedim..56.1307S. https://onlinelibrary.wiley.com/doi/full/10.1111/j.1365-3091.2008.01035.x. Retrieved 8 April 2023. 
  27. ↑ 27.0 27.1 Krencker, Francois-Nicolas; Fantasia, Alicia; Danisch, Jan; Martindale, Rowan; Kabiri, Lahcen; El Ouali, Mohamed; Bodin, Stéphane (September 2020). "Two-phased collapse of the shallow-water carbonate factory during the late Pliensbachian–Toarcian driven by changing climate and enhanced continental weathering in the Northwestern Gondwana Margin". Earth-Science Reviews 208: 103254. doi:10.1016/j.earscirev.2020.103254. Bibcode: 2020ESRv..20803254K. https://www.sciencedirect.com/science/article/abs/pii/S0012825220303007. Retrieved 14 May 2023. 
  28. ↑ Ruebsam, Wolfgang; Reolid, Matias; Sabatino, Nadia; Masetti, Daniele; Schwark, Lorenz (December 2020). "Molecular paleothermometry of the early Toarcian climate perturbation". Global and Planetary Change 195: 103351. doi:10.1016/j.gloplacha.2020.103351. Bibcode: 2020GPC...19503351R. 
  29. ↑ Ruebsam, Wolfgang; Al-Husseini, Moujahed (1 September 2021). "Orbitally synchronized late Pliensbachian–early Toarcian glacio-eustatic and carbon-isotope cycles". Palaeogeography, Palaeoclimatology, Palaeoecology 577: 110562. doi:10.1016/j.palaeo.2021.110562. Bibcode: 2021PPP...577k0562R. 
  30. ↑ Merkel, Anna; Munnecke, Axel (18 May 2023). "Glendonite-bearing concretions from the upper Pliensbachian (Lower Jurassic) of South Germany: indicators for a massive cooling in the European epicontinental sea". Facies 69 (3). doi:10.1007/s10347-023-00667-6. 
  31. ↑ Nordt, Lee; Breecker, Daniel; White, Joseph (30 December 2021). "Jurassic greenhouse ice-sheet fluctuations sensitive to atmospheric CO2 dynamics". Nature Geoscience 15 (1): 54–59. doi:10.1038/s41561-021-00858-2. https://www.nature.com/articles/s41561-021-00858-2#citeas. Retrieved 16 August 2023. 
  32. ↑ Suan, Guillaume; Mattioli, Emanuela; Pittet, Bernard; Lécuyer, Christophe; Suchéras-Marx, Baptiste; Duarte, Luís Vítor; Philippe, Marc; Reggiani, Letizia et al. (20 February 2010). "Secular environmental precursors to Early Toarcian (Jurassic) extreme climate changes". Earth and Planetary Science Letters 290 (3–4): 448–458. doi:10.1016/j.epsl.2009.12.047. Bibcode: 2010E&PSL.290..448S. https://www.sciencedirect.com/science/article/abs/pii/S0012821X10000117. Retrieved 19 August 2022. 
  33. ↑ Ruebsam, Wolfgang; Reolid, Matías; Schwark, Lorenz (10 January 2020). "δ13C of terrestrial vegetation records Toarcian CO2 and climate gradients". Scientific Reports 10 (1): 117. doi:10.1038/s41598-019-56710-6. PMID 31924807. Bibcode: 2020NatSR..10..117R. 
  34. ↑ Piazza, Veronica; Ullmann, Clemens Vinzenz; Aberhan, Martin (9 December 2020). "Ocean warming affected faunal dynamics of benthic invertebrate assemblages across the Toarcian Oceanic Anoxic Event in the Iberian Basin (Spain)". PLOS ONE 15 (12): e0242331. doi:10.1371/journal.pone.0242331. PMID 33296368. Bibcode: 2020PLoSO..1542331P. 
  35. ↑ Font, Eric; Duarte, Luís Vítor; Dekkers, Mark J.; Remazeilles, Celine; Egli, Ramon; Spangenberg, Jorge E.; Fantasia, Alicia; Ribeiro, Joana et al. (14 March 2022). "Rapid light carbon releases and increased aridity linked to Karoo-Ferrar magmatism during the early Toarcian oceanic anoxic event". Scientific Reports 12 (1): 4342. doi:10.1038/s41598-022-08269-y. PMID 35288615. Bibcode: 2022NatSR..12.4342F. 
  36. ↑ Riley, T. R.; Millar, I. L.; Watkeys, M. K.; Curtis, M. L.; Leat, P. T.; Klausen, M. B.; Fanning, C. M. (1 July 2004). "U–Pb zircon (SHRIMP) ages for the Lebombo rhyolites, South Africa: refining the duration of Karoo volcanism". Journal of the Geological Society 161 (4): 547–550. doi:10.1144/0016-764903-181. Bibcode: 2004JGSoc.161..547R. https://pubs.geoscienceworld.org/jgs/article-abstract/161/4/547/94306/U-Pb-zircon-SHRIMP-ages-for-the-Lebombo-rhyolites?redirectedFrom=fulltext. Retrieved 17 April 2023. 
  37. ↑ Svensen, Henrik; Corfu, Fernando; Polteau, Stéphane; Hammer, Øyvind; Planke, Sverre (1 April 2012). "Rapid magma emplacement in the Karoo Large Igneous Province". Earth and Planetary Science Letters 325-326: 1–9. doi:10.1016/j.epsl.2012.01.015. Bibcode: 2012E&PSL.325....1S. https://www.sciencedirect.com/science/article/abs/pii/S0012821X12000258. Retrieved 14 June 2023. 
  38. ↑ Burgess, S. D.; Bowring, S. A.; Fleming, T. H.; Elliot, D. H. (1 April 2015). "High-precision geochronology links the Ferrar large igneous province with early-Jurassic ocean anoxia and biotic crisis". Earth and Planetary Science Letters 415: 90–99. doi:10.1016/j.epsl.2015.01.037. Bibcode: 2015E&PSL.415...90B. https://www.sciencedirect.com/science/article/abs/pii/S0012821X15000655. Retrieved 14 June 2023. 
  39. ↑ Corfu, Fernando; Svensen, Henrik; Mazzini, A. (15 January 2016). "Comment to paper: Evaluating the temporal link between the Karoo LIP and climatic–biologic events of the Toarcian Stage with high-precision U–Pb geochronology by Bryan Sell, Maria Ovtcharova, Jean Guex, Annachiara Bartolini, Fred Jourdan, Jorge E. Spangenberg, Jean-Claude Vicente, Urs Schaltegger in Earth and Planetary Science Letters 408 (2014) 48–56". Earth and Planetary Science Letters 434: 349–352. doi:10.1016/j.epsl.2015.07.010. Bibcode: 2016E&PSL.434..349C. https://www.sciencedirect.com/science/article/abs/pii/S0012821X15004379. Retrieved 14 June 2023. 
  40. ↑ Moulin, Maud; Fluteau, Frédéric; Courtillot, Vincent; Marsh, Julian; Delpech, Guillaume; Quidelleur, Xavier; Gérard, Martine; Jay, Anne E. (13 July 2011). "An attempt to constrain the age, duration, and eruptive history of the Karoo flood basalt: Naude's Nek section (South Africa)" (in en). Journal of Geophysical Research 116 (B7): 1–27. doi:10.1029/2011JB008210. ISSN 0148-0227. http://doi.wiley.com/10.1029/2011JB008210. Retrieved 26 November 2023. 
  41. ↑ Percival, L. M. E.; Cohen, A. S.; Davies, M. K.; Dickson, A. J.; Hesselbo, Stephen P.; Jenkyns, Hugh C.; Leng, M. J.; Mather, Tamsin A. et al. (1 September 2016). "Osmium isotope evidence for two pulses of increased continental weathering linked to Early Jurassic volcanism and climate change". Geology 44 (9): 759–762. doi:10.1130/G37997.1. Bibcode: 2016Geo....44..759P. 
  42. ↑ Percival, Lawrence M. E.; Witt, M. L. I.; Mather, Tamsin A.; Hermoso, M.; Jenkyns, Hugh C.; Hesselbo, Stephen P.; Al-Suwaidi, A. H.; Storm, M. S. et al. (15 October 2015). "Globally enhanced mercury deposition during the end-Pliensbachian extinction and Toarcian OAE: A link to the Karoo–Ferrar Large Igneous Province". Earth and Planetary Science Letters 428: 267–280. doi:10.1016/j.epsl.2015.06.064. Bibcode: 2015E&PSL.428..267P. https://www.sciencedirect.com/science/article/pii/S0012821X15004276. Retrieved 28 March 2023. 
  43. ↑ Fantasia, Alicia; Adatte, Thierry; Spangenberg, Jorge E.; Font, Eric; Duarte, Luís V.; Föllmi, Karl B. (November 2019). "Global versus local processes during the Pliensbachian–Toarcian transition at the Peniche GSSP, Portugal: A multi-proxy record". Earth-Science Reviews 198: 102932. doi:10.1016/j.earscirev.2019.102932. Bibcode: 2019ESRv..19802932F. https://www.sciencedirect.com/science/article/abs/pii/S0012825219303289. Retrieved 29 March 2023. 
  44. ↑ 44.0 44.1 Fantasia, Alicia; Föllmi, Karl B.; Adatte, Thierry; Bernárdez, Enrique; Spangenberg, Jorge E.; Mattioli, Emanuela (10 August 2018). "The Toarcian Oceanic Anoxic Event in southwestern Gondwana: an example from the Andean Basin, northern Chile". Journal of the Geological Society 175 (6): 883–902. doi:10.1144/jgs2018-008. Bibcode: 2018JGSoc.175..883F. https://pubs.geoscienceworld.org/jgs/article-abstract/175/6/883/536768/The-Toarcian-Oceanic-Anoxic-Event-in-southwestern. Retrieved 29 March 2023. 
  45. ↑ Them II, T. R.; Jagoe, C. H.; Caruthers, A. H.; Gill, B. C.; Grasby, Stephen E.; Gröcke, D. R.; Yin, R.; Owens, J. D. (1 February 2019). "Terrestrial sources as the primary delivery mechanism of mercury to the oceans across the Toarcian Oceanic Anoxic Event (Early Jurassic)". Earth and Planetary Science Letters 507: 62–72. doi:10.1016/j.epsl.2018.11.029. Bibcode: 2019E&PSL.507...62T. 
  46. ↑ Ruhl, Micha; Hesselbo, Stephen P.; Jenkyns, Hugh C.; Xu, Weimu; Silva, Ricardo L.; Matthews, Kara J.; Mather, Tamsin A.; Niocaill, Conall Mac et al. (9 September 2022). "Reduced plate motion controlled timing of Early Jurassic Karoo-Ferrar large igneous province volcanism". Science Advances 8 (36): eabo0866. doi:10.1126/sciadv.abo0866. PMID 36083904. Bibcode: 2022SciA....8O.866R. 
  47. ↑ De Lena, Luis F.; Taylor, David; Guex, Jean; Bartolini, Annachiara; Adatte, Thierry; Van Acken, David; Spangenberg, Jorge E.; Samankassou, Elias et al. (5 December 2019). "The driving mechanisms of the carbon cycle perturbations in the late Pliensbachian (Early Jurassic)". Scientific Reports 9 (1): 18430. doi:10.1038/s41598-019-54593-1. PMID 31804521. 
  48. ↑ McElwain, Jennifer C.; Wade-Murphy, Jessica; Hesselbo, Stephen P. (26 May 2005). "Changes in carbon dioxide during an oceanic anoxic event linked to intrusion into Gondwana coals". Nature 435 (7041): 479–482. doi:10.1038/nature03618. PMID 15917805. Bibcode: 2005Natur.435..479M. https://www.nature.com/articles/nature03618?error=cookies_not_supported&code=2345c781-b851-4d01-bcef-5615f1252f11. Retrieved 7 January 2023. 
  49. ↑ Svensen, Henrik; Planke, Sverre; Chevallier, Luc; Malthe-Sørenssen, Anders; Corfu, Fernando; Jamtveit, Bjørn (30 April 2007). "Hydrothermal venting of greenhouse gases triggering Early Jurassic global warming". Earth and Planetary Science Letters 256 (3–4): 554–566. doi:10.1016/j.epsl.2007.02.013. Bibcode: 2007E&PSL.256..554S. https://www.sciencedirect.com/science/article/abs/pii/S0012821X07000763. Retrieved 20 January 2023. 
  50. ↑ Hesselbo, Stephen P.; Gröcke, Darren R.; Jenkyns, Hugh C.; Bjerrum, Christian J.; Farrimond, Paul; Morgans-Bell, Helen S.; Green, Owen R. (27 July 2000). "Massive dissociation of gas hydrate during a Jurassic oceanic anoxic event". Nature 406 (6794): 392–395. doi:10.1038/35019044. PMID 10935632. Bibcode: 2000Natur.406..392H. https://www.nature.com/articles/35019044?error=cookies_not_supported&code=6443966f-d7bf-436b-89df-9beee4f58c77. Retrieved 7 January 2023. 
  51. ↑ 51.0 51.1 Cohen, Anthony S.; Coe, Angela L.; Kemp, David B. (15 October 2007). "The Late Palaeocene–Early Eocene and Toarcian (Early Jurassic) carbon isotope excursions: a comparison of their time scales, associated environmental changes, causes and consequences". Journal of the Geological Society 163 (6): 1093–1108. doi:10.1144/0016-76492006-123. Bibcode: 2007JGSoc.164.1093C. https://www.lyellcollection.org/doi/10.1144/0016-76492006-123. Retrieved 20 January 2023. 
  52. ↑ Remírez, Mariano N.; Algeo, Thomas J. (October 2020). "Carbon-cycle changes during the Toarcian (Early Jurassic) and implications for regional versus global drivers of the Toarcian oceanic anoxic event". Earth-Science Reviews 209: 103283. doi:10.1016/j.earscirev.2020.103283. Bibcode: 2020ESRv..20903283R. https://www.sciencedirect.com/science/article/abs/pii/S0012825220303299. Retrieved 23 June 2023. 
  53. ↑ Ikeda, Masayuki; Hori, Rie S.; Ikehara, Minoru; Miyashita, Ren; Chino, Masashi; Yamada, Kazuyoshi (November 2018). "Carbon cycle dynamics linked with Karoo-Ferrar volcanism and astronomical cycles during Pliensbachian-Toarcian (Early Jurassic)". Global and Planetary Change 170: 163–171. doi:10.1016/j.gloplacha.2018.08.012. Bibcode: 2018GPC...170..163I. https://www.sciencedirect.com/science/article/abs/pii/S0921818118302698. Retrieved 14 June 2023. 
  54. ↑ Kemp, David B.; Coe, Angela L.; Cohen, Anthony S.; Weedon, Graham P. (1 November 2011). "Astronomical forcing and chronology of the early Toarcian (Early Jurassic) oceanic anoxic event in Yorkshire, UK". Paleoceanography and Paleoclimatology 26 (4): 1–17. doi:10.1029/2011PA002122. Bibcode: 2011PalOc..26.4210K. 
  55. ↑ McArthur, J. M.; Cohen, A. S.; Coe, A. L.; Kemp, David B.; Bailey, R. J.; Smith, D. G. (5 June 2008). "Discussion on the Late Palaeocene–Early Eocene and Toarcian (Early Jurassic) carbon isotope excursions: a comparison of their time scales, associated environmental change, causes and consequencesJournal, Vol. 164, 2007, 1093–1108". Journal of the Geological Society 165 (4): 875–880. doi:10.1144/0016-76492007-157. Bibcode: 2008JGSoc.165..875M. https://www.lyellcollection.org/doi/10.1144/0016-76492007-157. Retrieved 20 January 2023. 
  56. ↑ Van de Schootbrugge, B.; McArthur, J. M.; Bailey, T. R.; Rosenthal, Y.; Wright, J. D.; Miller, K. G. (26 August 2005). "Toarcian oceanic anoxic event: An assessment of global causes using belemnite C isotope records". Paleoceanography and Paleoclimatology 20 (3): 1–10. doi:10.1029/2004PA001102. Bibcode: 2005PalOc..20.3008V. https://agupubs.onlinelibrary.wiley.com/doi/10.1029/2004PA001102. Retrieved 7 January 2023. 
  57. ↑ Beerling, David J.; Lomas, M. R.; Gröcke, Darren R. (January 2002). "On the nature of methane gas-hydrate dissociation during the Toarcian and Aptian Oceanic anoxic events". American Journal of Science 302 (1): 28–49. doi:10.2475/ajs.302.1.28. Bibcode: 2002AmJS..302...28B. https://www.ajsonline.org/content/302/1/28. Retrieved 7 January 2023. 
  58. ↑ Wignall, Paul B.; Newton, Robert J.; Little, Crispin T. S. (December 2005). "The timing of paleoenvironmental change and cause-and-effect relationships during the early Jurassic mass extinction in Europe". American Journal of Science 305 (10): 1014–1032. doi:10.2475/ajs.305.10.1014. Bibcode: 2005AmJS..305.1014W. https://www.ajsonline.org/content/305/10/1014. Retrieved 7 January 2023. 
  59. ↑ Heimdal, Thea H.; Goddéris, Yves; Jones, Morgan T.; Svensen, Henrik H. (28 October 2021). "Assessing the importance of thermogenic degassing from the Karoo Large Igneous Province (LIP) in driving Toarcian carbon cycle perturbations". Nature Communications 12 (1): 6221. doi:10.1038/s41467-021-26467-6. PMID 34711826. Bibcode: 2021NatCo..12.6221H. 
  60. ↑ Krencker, François-Nicolas; Lindström, Sofie; Bodin, Stéphane (29 August 2019). "A major sea-level drop briefly precedes the Toarcian oceanic anoxic event: implication for Early Jurassic climate and carbon cycle". Scientific Reports 9 (1): 12518. doi:10.1038/s41598-019-48956-x. PMID 31467345. Bibcode: 2019NatSR...912518K. 
  61. ↑ Ruebsam, Wolfgang; Reolid, Matías; Schwark, Lorenz (10 January 2020). "δ13C of terrestrial vegetation records Toarcian CO2 and climate gradients". Scientific Reports 10 (1): 117. doi:10.1038/s41598-019-56710-6. PMID 31924807. Bibcode: 2020NatSR..10..117R. 
  62. ↑ Ruebsam, Wolfgang; Mayer, Bernhard; Schwark, Lorenz (January 2019). "Cryosphere carbon dynamics control early Toarcian global warming and sea level evolution". Global and Planetary Change 172: 440–453. doi:10.1016/j.gloplacha.2018.11.003. Bibcode: 2019GPC...172..440R. https://www.sciencedirect.com/science/article/abs/pii/S0921818118305009. Retrieved 7 January 2023. 
  63. ↑ Ruebsam, Wolfgang; Reolid, Matías; Marok, Abbas; Schwark, Lorenz (April 2020). "Drivers of benthic extinction during the early Toarcian (Early Jurassic) at the northern Gondwana paleomargin: Implications for paleoceanographic conditions". Earth-Science Reviews 203: 103117. doi:10.1016/j.earscirev.2020.103117. Bibcode: 2020ESRv..20303117R. https://www.sciencedirect.com/science/article/abs/pii/S0012825219306841. Retrieved 14 May 2023. 
  64. ↑ Kemp, David B.; Izumi, Kentaro (15 November 2014). "Multiproxy geochemical analysis of a Panthalassic margin record of the early Toarcian oceanic anoxic event (Toyora area, Japan)". Palaeogeography, Palaeoclimatology, Palaeoecology 414: 332–341. doi:10.1016/j.palaeo.2014.09.019. Bibcode: 2014PPP...414..332K. https://www.sciencedirect.com/science/article/pii/S003101821400474X. Retrieved 8 January 2023. 
  65. ↑ Tremolada, Fabrizio; Van de Schootbrugge, Bas; Erba, Elisabetta (3 June 2005). "Early Jurassic schizosphaerellid crisis in Cantabria, Spain: Implications for calcification rates and phytoplankton evolution across the Toarcian oceanic anoxic event". Paleoceanography and Paleoclimatology 20 (2): 1–11. doi:10.1029/2004PA001120. Bibcode: 2005PalOc..20.2011T. 
  66. ↑ Rodrigues, Bruno; Duarte, Luís V.; Silva, Ricardo L.; Mendonça Filho, João Graciano (15 September 2020). "Sedimentary organic matter and early Toarcian environmental changes in the Lusitanian Basin (Portugal)". Palaeogeography, Palaeoclimatology, Palaeoecology 554: 109781. doi:10.1016/j.palaeo.2020.109781. Bibcode: 2020PPP...554j9781R. https://www.sciencedirect.com/science/article/abs/pii/S0031018220302261. Retrieved 27 September 2022. 
  67. ↑ Rodrigues, Bruno; Silva, Ricardo L.; Mendonça Filho, João Graciano; Comas-Rengifo, María J.; Goy, Antonio; Duarte, Luís V. (1 September 2020). "Kerogen assemblages and δ13CKerogen of the uppermost Pliensbachian–lower Toarcian succession of the Asturian Basin (northern Spain)". International Journal of Coal Geology 229: 103573. doi:10.1016/j.coal.2020.103573. Bibcode: 2020IJCG..22903573R. https://www.sciencedirect.com/science/article/abs/pii/S0166516220305693. Retrieved 14 May 2023. 
  68. ↑ Brazier, Jean-Michel; Suan, Guillaume; Tacail, Théo; Simon, Laurent; Martin, Jeremy E.; Mattioli, Emanuela; Balter, Vincent (1 February 2015). "Calcium isotope evidence for dramatic increase of continental weathering during the Toarcian oceanic anoxic event (Early Jurassic)". Earth and Planetary Science Letters 411: 164–176. doi:10.1016/j.epsl.2014.11.028. ISSN 0012-821X. https://www.sciencedirect.com/science/article/pii/S0012821X14007201. Retrieved 26 November 2023. 
  69. ↑ 69.0 69.1 Slater, Sam M.; Twitchett, Richard J.; Danise, Silvia; Vajda, Vivi (29 April 2019). "Substantial vegetation response to Early Jurassic global warming with impacts on oceanic anoxia". Nature Geoscience 12 (6): 462–467. doi:10.1038/s41561-019-0349-z. Bibcode: 2019NatGe..12..462S. https://www.nature.com/articles/s41561-019-0349-z?error=cookies_not_supported&code=9b2cf5a2-6cd7-4d1f-be00-ee8b1c0e1073. Retrieved 17 December 2022. 
  70. ↑ Ruban, Dmitry A. (2004). "Diversity dynamics of Early-Middle Jurassic brachiopods of Caucasus, and the Pliensbachian-Toarcian mass extinction". Acta Palaeontologica Polonica 49 (2): 275–282. https://agro.icm.edu.pl/agro/element/bwmeta1.element.agro-article-5947f3c1-bfa8-4a98-a570-6bcde6300eaa. Retrieved 14 May 2023. 
  71. ↑ Harazim, Dario; Van de Schootbrugge, Bas; Sorichter, Katrin; Fiebig, Jens; Weug, Andries; Suan, Guillaume; Oschmann, Wolfgang (21 August 2012). "Spatial variability of watermass conditions within the European Epicontinental Seaway during the Early Jurassic (Pliensbachian–Toarcian)". Sedimentology 60 (2): 359–390. doi:10.1111/j.1365-3091.2012.01344.x. https://onlinelibrary.wiley.com/doi/full/10.1111/j.1365-3091.2012.01344.x. Retrieved 8 April 2023. 
  72. ↑ Dera, Guillaume; Donnadieu, Yannick (13 June 2012). "Modeling evidences for global warming, Arctic seawater freshening, and sluggish oceanic circulation during the Early Toarcian anoxic event". Paleoceanography and Paleoclimatology 27 (2): 1–15. doi:10.1029/2012PA002283. Bibcode: 2012PalOc..27.2211D. 
  73. ↑ Arias, Carmen (8 August 2007). "Pliensbachian–Toarcian ostracod biogeography in NW Europe: Evidence for water mass structure evolution". Palaeogeography, Palaeoclimatology, Palaeoecology 251 (3): 398–421. doi:10.1016/j.palaeo.2007.04.014. ISSN 0031-0182. https://www.sciencedirect.com/science/article/pii/S0031018207002398. Retrieved 26 November 2023. 
  74. ↑ Baranyi, Viktória; Pálfy, József; Görög, Ágnes; Riding, James B.; Raucsik, Béla (1 December 2016). "Multiphase response of palynomorphs to the Toarcian Oceanic Anoxic Event (Early Jurassic) in the Réka Valley section, Hungary". Review of Palaeobotany and Palynology 235: 51–70. doi:10.1016/j.revpalbo.2016.09.011. ISSN 0034-6667. https://www.sciencedirect.com/science/article/pii/S0034666715300099. Retrieved 26 November 2023. 
  75. ↑ Ruebsam, Wolfgang; Mattioli, Emanuela; Schwark, Lorenz (October 2022). "Weakening of the biological pump induced by a biocalcification crisis during the early Toarcian Oceanic Anoxic Event". Global and Planetary Change 217. doi:10.1016/j.gloplacha.2022.103954. https://www.sciencedirect.com/science/article/abs/pii/S0921818122002211. Retrieved 5 August 2023. 
  76. ↑ Li, Binbing; Jin, Xin; Corso, Jacopo Dal; Ogg, James G.; Lang, Xianguo; Baranyi, Viktória; Preto, Nereo; Franceschi, Marco et al. (1 February 2023). "Complex pattern of environmental changes and organic matter preservation in the NE Ordos lacustrine depositional system (China) during the T-OAE (Early Jurassic)". Global and Planetary Change 221: 104045. doi:10.1016/j.gloplacha.2023.104045. ISSN 0921-8181. https://www.sciencedirect.com/science/article/pii/S0921818123000188. Retrieved 26 November 2023. 
  77. ↑ Xu, Weimu; Weijers, Johan W. H.; Ruhl, Micha; Idiz, Erdem F.; Jenkyns, Hugh C.; Riding, James B.; Gorbanenko, Olga; Hesselbo, Stephen B. (3 November 2021). "Molecular and petrographical evidence for lacustrine environmental and biotic change in the palaeo-Sichuan mega-lake (China) during the Toarcian Oceanic Anoxic Event". Carbon Cycle and Ecosystem Response to the Jenkyns Event in the Early Toarcian (Jurassic). The Geological Society of London. doi:10.1144/SP514-2021-2. ISBN 9781786209993. https://pubs.geoscienceworld.org/gsl/books/edited-volume/2338/chapter-abstract/132175319/Molecular-and-petrographical-evidence-for?redirectedFrom=fulltext. Retrieved 26 November 2023. 
  78. ↑ Suan, Guillaume; Schöllhorn, Iris; Schlögl, Ján; Segit, Tomasz; Mattioli, Emanuela; Lécuyer, Christophe; Fourel, François (November 2018). "Euxinic conditions and high sulfur burial near the European shelf margin (Pieniny Klippen Belt, Slovakia) during the Toarcian oceanic anoxic event" (in en). Global and Planetary Change 170: 246–259. doi:10.1016/j.gloplacha.2018.09.003. Bibcode: 2018GPC...170..246S. https://www.sciencedirect.com/science/article/abs/pii/S0921818118302017. Retrieved 26 March 2023. 
  79. ↑ Them II, T. R.; Owens, J. D.; Marroquín, S. M.; Caruthers, Andrew H.; Trabucho Alexandre, J. P.; Gill, B. C. (22 November 2022). "Reduced Marine Molybdenum Inventory Related to Enhanced Organic Carbon Burial and an Expansion of Reducing Environments in the Toarcian (Early Jurassic) Oceans". AGU Advances 3 (6). doi:10.1029/2022AV000671. https://agupubs.onlinelibrary.wiley.com/doi/full/10.1029/2022AV000671. Retrieved 16 August 2023. 
  80. ↑ Gibson, Alexander J.; Gill, Benjamin C.; Ruhl, Micha; Jenkyns, Hugh C.; Porcelli, Donald; Idiz, Erdem; Lyons, Timothy W.; Van den Boorn, Sander H. J. M. (27 June 2017). "Molybdenum-isotope chemostratigraphy and paleoceanography of the Toarcian Oceanic Anoxic Event (Early Jurassic)". Paleoceanography and Paleoclimatology 32 (8): 813–829. doi:10.1002/2016PA003048. Bibcode: 2017PalOc..32..813D. 
  81. ↑ Fernández-Martínez, Javier; Martínez Ruíz, Francisca; Rodríguez-Tovar, Francisco J.; Piñuela, Laura; García-Ramos, José C.; Algeo, Thomas J. (February 2023). "Euxinia and hydrographic restriction in the Tethys Ocean: Reassessing global oceanic anoxia during the early Toarcian". Global and Planetary Change 221: 104026. doi:10.1016/j.gloplacha.2022.104026. Bibcode: 2023GPC...22104026F. https://www.sciencedirect.com/science/article/abs/pii/S0921818122002934. Retrieved 2 April 2023. 
  82. ↑ Baroni, Itzel Ruvalcaba; Pohl, Alexandre; Van Helmond, Niels A. G. M.; Papadomanolaki, Nina M.; Coe, Angela L.; Cohen, Anthony S.; Van de Schootbrugge, Bas; Donnadieu, Yannick et al. (25 August 2018). "Ocean Circulation in the Toarcian (Early Jurassic): A Key Control on Deoxygenation and Carbon Burial on the European Shelf". Paleoceanography and Paleoclimatology 33 (9): 994–1012. doi:10.1029/2018PA003394. Bibcode: 2018PaPa...33..994R. 
  83. ↑ Chen, Wenhan; Kemp, David B.; He, Tianchen; Newton, Robert J.; Xiong, Yijun; Jenkyns, Hugh C.; Izumi, Kentaro; Cho, Tenichi et al. (15 January 2023). "Shallow- and deep-ocean Fe cycling and redox evolution across the Pliensbachian–Toarcian boundary and Toarcian Oceanic Anoxic Event in Panthalassa". Earth and Planetary Science Letters 602: 117959. doi:10.1016/j.epsl.2022.117959. Bibcode: 2023E&PSL.60217959C. https://www.sciencedirect.com/science/article/abs/pii/S0012821X22005957. Retrieved 14 May 2023. 
  84. ↑ Kunert, Alexandra; Kendall, Brian (13 February 2023). "Global ocean redox changes before and during the Toarcian Oceanic Anoxic Event". Nature Communications 14 (1): 815. doi:10.1038/s41467-023-36516-x. PMID 36781894. PMC 9925726. Bibcode: 2023NatCo..14..815K. https://www.researchgate.net/publication/368472355. Retrieved 23 June 2023. 
  85. ↑ Mattioli, Emanuela; Pittet, Bernard; Palliani, Raffaella Bucefalo; Röhl, Hans-Joachim; Schmid-Röhl, Annette; Morettini, Elena (1 July 2004). "Phytoplankton evidence for the timing and correlation of palaeoceanographical changes during the early Toarcian oceanic anoxic event (Early Jurassic)". Journal of the Geological Society 161 (4): 685–693. doi:10.1144/0016-764903-074. Bibcode: 2004JGSoc.161..685M. https://pubs.geoscienceworld.org/jgs/article-abstract/161/4/685/94337/Phytoplankton-evidence-for-the-timing-and. Retrieved 29 March 2023. 
  86. ↑ Trecalli, Alberto; Spangenberg, Jorge; Adatte, Thierry; Föllmi, Karl B.; Parente, Mariano (December 2012). "Carbonate platform evidence of ocean acidification at the onset of the early Toarcian oceanic anoxic event" (in en). Earth and Planetary Science Letters 357-358: 214–225. doi:10.1016/j.epsl.2012.09.043. Bibcode: 2012E&PSL.357..214T. https://linkinghub.elsevier.com/retrieve/pii/S0012821X12005390. 
  87. ↑ Ettinger, Nicholas P.; Larson, Toti E.; Kerans, Charles; Thibodeau, Alyson M.; Hattori, Kelly E.; Kacur, Sean M.; Martindale, Rowan C. (23 September 2020). Eberli, Gregor. ed. "Ocean acidification and photic‐zone anoxia at the Toarcian Oceanic Anoxic Event: Insights from the Adriatic Carbonate Platform" (in en). Sedimentology 68: 63–107. doi:10.1111/sed.12786. ISSN 0037-0746. https://onlinelibrary.wiley.com/doi/10.1111/sed.12786. 
  88. ↑ Papadomanolaki, Nina M.; Lenstra, Wytze K.; Wolthers, Mariette; Slomp, Caroline P. (1 July 2022). "Enhanced phosphorus recycling during past oceanic anoxia amplified by low rates of apatite authigenesis". Science Advances 8 (26): eabn2370. doi:10.1126/sciadv.abn2370. PMID 35776794. Bibcode: 2022SciA....8N2370P. 
  89. ↑ Chen, Wenhan; Kemp, David B.; He, Tianchen; Huang, Chunju; Jin, Simin; Xiong, Yijun; Newton, Robert J. (1 December 2021). "First record of the early Toarcian Oceanic Anoxic Event in the Hebrides Basin (UK) and implications for redox and weathering changes". Global and Planetary Change 207: 103685. doi:10.1016/j.gloplacha.2021.103685. ISSN 0921-8181. https://www.sciencedirect.com/science/article/pii/S0921818121002708. Retrieved 26 November 2023. 
  90. ↑ 90.0 90.1 Krencker, François-Nicolas; Bodin, Stéphane; Suan, Guillaume; Heimhofer, Ulrich; Kabiri, Lahcen; Immenhauser, Adrian (1 September 2015). "Toarcian extreme warmth led to tropical cyclone intensification". Earth and Planetary Science Letters 425: 120–130. doi:10.1016/j.epsl.2015.06.003. Bibcode: 2015E&PSL.425..120K. https://www.sciencedirect.com/science/article/abs/pii/S0012821X15003532. Retrieved 20 January 2023. 
  91. ↑ Hesselbo, Stephen P.; Jenkyns, Hugh C.; Duarte, Luis V.; Oliveira, Luiz C. V. (30 January 2007). "Carbon-isotope record of the Early Jurassic (Toarcian) Oceanic Anoxic Event from fossil wood and marine carbonate (Lusitanian Basin, Portugal)". Earth and Planetary Science Letters 253 (3–4): 455–470. doi:10.1016/j.epsl.2006.11.009. Bibcode: 2007E&PSL.253..455H. https://www.sciencedirect.com/science/article/abs/pii/S0012821X06007965. Retrieved 11 January 2023. 
  92. ↑ Neumeister, S.; Gratzer, R.; Algeo, Thomas J.; Bechtel, A.; Gawlick, H.-J.; Newton, Robert J.; Sachsenhofer, R. F. (March 2015). "Oceanic response to Pliensbachian and Toarcian magmatic events: Implications from an organic-rich basinal succession in the NW Tethys". Global and Planetary Change 126: 62–83. doi:10.1016/j.gloplacha.2015.01.007. Bibcode: 2015GPC...126...62N. https://www.sciencedirect.com/science/article/abs/pii/S0921818115000235. Retrieved 8 January 2023. 
  93. ↑ Kafousia, N.; Karakitsios, V.; Jenkyns, Hugh C.; Mattioli, E. (22 February 2011). "A global event with a regional character: the Early Toarcian Oceanic Anoxic Event in the Pindos Ocean (northern Peloponnese, Greece)". Geological Magazine 148 (4): 619–631. doi:10.1017/S0016756811000082. Bibcode: 2011GeoM..148..619K. https://www.cambridge.org/core/journals/geological-magazine/article/abs/global-event-with-a-regional-character-the-early-toarcian-oceanic-anoxic-event-in-the-pindos-ocean-northern-peloponnese-greece/55263029D8279B48E4F3DC926587F0A4. Retrieved 13 March 2023. 
  94. ↑ Alnazghah, Mahmoud; Koeshidayatullah, Ardiansyah; Al-Hussaini, Abdulkarim; Amao, Abduljamiu; Song, Haijun; Al-Ramadan, Khalid (27 October 2022). "Evidence for the early Toarcian Carbon Isotope Excursion (T-CIE) from the shallow marine siliciclastic red beds of Arabia". Scientific Reports 12 (1): 18124. doi:10.1038/s41598-022-21716-0. PMID 36302804. Bibcode: 2022NatSR..1218124A. 
  95. ↑ 95.0 95.1 Jin, Xin; Shi, Zhiqiang; Baranyi, Viktória; Kemp, David B.; Han, Zhong; Luo, Genming; Hu, Jianfang; He, Feng et al. (October 2020). "The Jenkyns Event (early Toarcian OAE) in the Ordos Basin, North China". Global and Planetary Change 193: 103273. doi:10.1016/j.gloplacha.2020.103273. Bibcode: 2020GPC...19303273J. https://www.sciencedirect.com/science/article/abs/pii/S0921818120301648. Retrieved 14 May 2023. 
  96. ↑ Mazzini, Adriano; Svensen, Henrik; Leanza, Héctor A.; Corfu, Fernando; Planke, Sverre (1 September 2010). "Early Jurassic shale chemostratigraphy and U–Pb ages from the Neuquén Basin (Argentina): Implications for the Toarcian Oceanic Anoxic Event". Earth and Planetary Science Letters 297 (3–4): 633–645. doi:10.1016/j.epsl.2010.07.017. Bibcode: 2010E&PSL.297..633M. https://www.sciencedirect.com/science/article/abs/pii/S0012821X10004553. Retrieved 14 May 2023. 
  97. ↑ Jenkyns, Hugh C. (February 1998). "The early Toarcian ( Jurassic) anoxic event: stratigraphic, sedimentary, and geochemical evidence". American Journal of Science 288 (2): 101–151. doi:10.2475/ajs.288.2.101. https://www.researchgate.net/publication/277467795. Retrieved 4 January 2023. 
  98. ↑ Martinez, Mathieu; Dera, Guillaume (13 October 2015). "Orbital pacing of carbon fluxes by a ∼9-My eccentricity cycle during the Mesozoic" (in en). Proceedings of the National Academy of Sciences of the United States of America 112 (41): 12604–12609. doi:10.1073/pnas.1419946112. ISSN 0027-8424. PMID 26417080. 
  99. ↑ Gill, Benjamin C.; Lyons, Timothy W.; Jenkyns, Hugh C. (15 December 2011). "A global perturbation to the sulfur cycle during the Toarcian Oceanic Anoxic Event". Earth and Planetary Science Letters 312 (3–4): 484–496. doi:10.1016/j.epsl.2011.10.030. Bibcode: 2011E&PSL.312..484G. https://www.sciencedirect.com/science/article/abs/pii/S0012821X1100625X. Retrieved 4 January 2023. 
  100. ↑ Chen, Wenhan; Kemp, David B.; Newton, Robert J.; He, Tianchen; Wang, Chunju; Cho, Tenichi; Izumi, Kentaro (August 2022). "Major sulfur cycle perturbations in the Panthalassic Ocean across the Pliensbachian-Toarcian boundary and the Toarcian Oceanic Anoxic Event". Global and Planetary Change 215: 103884. doi:10.1016/j.gloplacha.2022.103884. Bibcode: 2022GPC...21503884C. https://www.sciencedirect.com/science/article/abs/pii/S0921818122001515. Retrieved 25 March 2023. 
  101. ↑ Krencker, Francois-Nicolas; Fantasia, Alicia; Danisch, Jan; Martindale, Rowan; Kabiri, Lahcen; El Ouali, Mohamed; Bodin, Stéphane (2020). "Two-phased collapse of the shallow-water carbonate factory during the late Pliensbachian–Toarcian driven by changing climate and enhanced continental weathering in the Northwestern Gondwana Margin". Earth-Science Reviews 208: 103254. doi:10.1016/j.earscirev.2020.103254. Bibcode: 2020ESRv..20803254K. https://www.sciencedirect.com/science/article/abs/pii/S0012825220303007. Retrieved 17 December 2022. 
  102. ↑ Danise, Silvia; Clémence, Marie-Emilie; Price, Gregory D.; Murphy, Daniel P.; Gómez, Juan J.; Twitchett, Richard J. (15 June 2019). "Stratigraphic and environmental control on marine benthic community change through the early Toarcian extinction event (Iberian Range, Spain)". Palaeogeography, Palaeoclimatology, Palaeoecology 524: 183–200. doi:10.1016/j.palaeo.2019.03.039. Bibcode: 2019PPP...524..183D. https://www.sciencedirect.com/science/article/abs/pii/S0031018218309258. Retrieved 23 November 2022. 
  103. ↑ Vörös, Attila; Kocsis, Ádám; Pálfy, József (1 September 2016). "Demise of the last two spire-bearing brachiopod orders (Spiriferinida and Athyridida) at the Toarcian (Early Jurassic) extinction event". Palaeogeography, Palaeoclimatology, Palaeoecology 457: 233–241. doi:10.1016/j.palaeo.2016.06.022. Bibcode: 2016PPP...457..233V. https://www.sciencedirect.com/science/article/abs/pii/S0031018216302140#!. Retrieved 29 October 2022. 
  104. ↑ Joran, Fernando García; Baeza-Carratalá, José Francisco; Goy, Antonio (1 October 2018). "Changes in brachiopod body size prior to the Early Toarcian (Jurassic) Mass Extinction". Palaeogeography, Palaeoclimatology, Palaeoecology 506: 242–249. doi:10.1016/j.palaeo.2018.06.045. Bibcode: 2018PPP...506..242G. https://www.sciencedirect.com/science/article/abs/pii/S0031018218304644#!. Retrieved 29 October 2022. 
  105. ↑ Piazza, Veronica; Duarte, Luís Vítor; Renaudie, Johan; Aberhan, Martin (29 March 2019). "Reductions in body size of benthic macroinvertebrates as a precursor of the early Toarcian (Early Jurassic) extinction event in the Lusitanian Basin, Portugal". Paleobiology 45 (2): 296–316. doi:10.1017/pab.2019.11. Bibcode: 2019Pbio...45..296P. 
  106. ↑ Ullmann, C. V.; Boyle, R.; Duarte, Luís Vítor; Hesselbo, Stephen P.; Kasemann, S. A.; Klein, T.; Lenton, T. M.; Piazza, Veronica et al. (16 April 2020). "Warm afterglow from the Toarcian Oceanic Anoxic Event drives the success of deep-adapted brachiopods". Scientific Reports 10 (1): 6549. doi:10.1038/s41598-020-63487-6. PMID 32300235. Bibcode: 2020NatSR..10.6549U. 
  107. ↑ García Joral, Fernando; Goy, Antonio; Rosales, Idoia; Barnolas, Antonio; Sevillano, Ana; López-García, José María (5 September 2022). "Early Toarcian (Jurassic) brachiopods from the Balearic Islands (Spain) and their paleobiogeographic context". Journal of Iberian Geology 48 (4): 445–460. doi:10.1007/s41513-022-00197-0. 
  108. ↑ 108.0 108.1 Zakharov, V. A.; Shurygin, B. N.; Il’ina, V. I.; Nikitenko, B. L. (July 2006). "Pliensbachian-Toarcian biotic turnover in north Siberia and the Arctic region". Stratigraphy and Geological Correlation 14 (4): 399–417. doi:10.1134/S0869593806040046. Bibcode: 2006SGC....14..399Z. https://link.springer.com/article/10.1134/S0869593806040046?error=cookies_not_supported&code=d5ba4f95-176d-405e-8904-7d3cf0ec6db5. Retrieved 14 June 2023. 
  109. ↑ 109.0 109.1 Wignall, Paul B.; Bond, David P. G. (2008). "The end-Triassic and Early Jurassic mass extinction records in the British Isles". Proceedings of the Geologists' Association 119 (1): 73–84. doi:10.1016/S0016-7878(08)80259-3. Bibcode: 2008PrGA..119...73W. https://www.sciencedirect.com/science/article/abs/pii/S0016787808802593. Retrieved 23 November 2022. 
  110. ↑ Martindale, Rowan C.; Aberhan, Martin (15 July 2017). "Response of macrobenthic communities to the Toarcian Oceanic Anoxic Event in northeastern Panthalassa (Ya Ha Tinda, Alberta, Canada)". Palaeogeography, Palaeoclimatology, Palaeoecology 478: 103–120. doi:10.1016/j.palaeo.2017.01.009. Bibcode: 2017PPP...478..103M. https://www.sciencedirect.com/science/article/abs/pii/S0031018217300160. Retrieved 8 April 2023. 
  111. ↑ Morten, Simon D.; Twitchett, Richard J. (20 December 2009). "Fluctuations in the body size of marine invertebrates through the Pliensbachian–Toarcian extinction event". Palaeogeography, Palaeoclimatology, Palaeoecology 284 (1–2): 29–38. doi:10.1016/j.palaeo.2009.08.023. Bibcode: 2009PPP...284...29M. https://www.sciencedirect.com/science/article/abs/pii/S0031018209003472. Retrieved 14 June 2023. 
  112. ↑ Guex, Jean; Bartolini, Annachiara; Spangenberg, Jorge E.; Vicente, J.-C.; Schaltegger, Urs (19 September 2012). "Ammonoid multi-extinction crises during the Late Pliensbachian - Toarcian and carbon cycle instabilities". Solid Earth 4 (2): 1205–1228. doi:10.5194/sed-4-1205-2012. https://www.researchgate.net/publication/258723336. Retrieved 26 November 2023. 
  113. ↑ Dera, Guillaume; Neige, Pascal; Dommergues, Jean-Louis; Fara, Emmanuel; Laffont, Rémi; Pellenard, Pierre (January 2010). "High-resolution dynamics of Early Jurassic marine extinctions: the case of Pliensbachian–Toarcian ammonites (Cephalopoda)" (in en). Journal of the Geological Society 167 (1): 21–33. doi:10.1144/0016-76492009-068. ISSN 0016-7649. Bibcode: 2010JGSoc.167...21D. http://jgs.lyellcollection.org/lookup/doi/10.1144/0016-76492009-068. 
  114. ↑ 114.0 114.1 De Baets, Kenneth; Nätscher, Paulina S.; Rita, Patricia; Fara, Emmanuel; Neige, Pascal; Bardin, Jérémie; Dera, Guillaume; Duarte, Luís Vítor et al. (20 December 2021). "The impact of the Pliensbachian–Toarcian crisis on belemnite assemblages and size distribution". Swiss Journal of Palaeontology 140 (25): 1–14. doi:10.1186/s13358-021-00242-y. 
  115. ↑ Vasseur, R.; Lathuilière, B.; Lazăr, I.; Martindale, Rowan C.; Bodin, S.; Durlet, C. (December 2021). "Major coral extinctions during the early Toarcian global warming event". Global and Planetary Change 207: 103647. doi:10.1016/j.gloplacha.2021.103647. Bibcode: 2021GPC...20703647V. 
  116. ↑ Reolid, Matías; Emanuela, Mattioli; Nieto, Luis M.; Rodríguez-Tovar, Francisco J. (1 October 2014). "The Early Toarcian Oceanic Anoxic Event in the External Subbetic (Southiberian Palaeomargin, Westernmost Tethys): Geochemistry, nannofossils and ichnology". Palaeogeography, Palaeoclimatology, Palaeoecology 411: 79–94. doi:10.1016/j.palaeo.2014.06.023. ISSN 0031-0182. https://www.sciencedirect.com/science/article/pii/S0031018214003356. Retrieved 30 December 2023. 
  117. ↑ 117.0 117.1 Reolid, M.; Duarte, L. V.; Rita, P. (15 April 2019). "Changes in foraminiferal assemblages and environmental conditions during the T-OAE (Early Jurassic) in the northern Lusitanian Basin, Portugal". Palaeogeography, Palaeoclimatology, Palaeoecology 520: 30–43. doi:10.1016/j.palaeo.2019.01.022. Bibcode: 2019PPP...520...30R. https://www.sciencedirect.com/science/article/abs/pii/S0031018218308307. Retrieved 17 December 2022. 
  118. ↑ Goričan, Špela; Carter, Elizabeth S.; Guex, Jean; O’Dogherty, Luis; De Wever, Patrick; Dumitrica, Paulian; Hori, Rie S.; Matsuoka, Atsushi et al. (15 September 2013). "Evolutionary patterns and palaeobiogeography of Pliensbachian and Toarcian (Early Jurassic) Radiolaria". Palaeogeography, Palaeoclimatology, Palaeoecology 386: 620–636. doi:10.1016/j.palaeo.2013.06.028. https://www.sciencedirect.com/science/article/abs/pii/S0031018213003052. Retrieved 17 December 2022. 
  119. ↑ Hess, Silvia; Nagy, Jenő; Laursen, Gitte Vestergaard (28 January 2014). "Benthic foraminifera from the Lower Jurassic transgressive mudstones of the south-western Barents Sea—a possible high-latitude expression of the global Pliensbachian–Toarcian turnover?". Polar Research 33 (1): 20206. doi:10.3402/polar.v33.20206. 
  120. ↑ Reolid, Matías; Copestake, Philip; Johnson, Ben (15 October 2019). "Foraminiferal assemblages, extinctions and appearances associated with the Early Toarcian Oceanic Anoxic Event in the Llanbedr (Mochras Farm) Borehole, Cardigan Bay Basin, United Kingdom". Palaeogeography, Palaeoclimatology, Palaeoecology 532: 109277. doi:10.1016/j.palaeo.2019.109277. Bibcode: 2019PPP...532j9277R. https://www.sciencedirect.com/science/article/abs/pii/S0031018219303980. Retrieved 23 November 2022. 
  121. ↑ Müller, Tamás; Karancz, Szabina; Mattioli, Emanuela; Milovský, Rastislav; Pálfy, József; Schlögl, Jan; Segit, Tomasz; Šimo, Vladimír et al. (December 2020). "Assessing anoxia, recovery and carbonate production setback in a hemipelagic Tethyan basin during the Toarcian Oceanic Anoxic Event (Western Carpathians)". Global and Planetary Change 195: 103366. doi:10.1016/j.gloplacha.2020.103366. Bibcode: 2020GPC...19503366M. 
  122. ↑ Danise, Silvia; Twitchett, Richard J.; Little, Crispin T. S.; Clémence, Marie-Emilie (14 February 2013). "The Impact of Global Warming and Anoxia on Marine Benthic Community Dynamics: an Example from the Toarcian (Early Jurassic)". PLoS ONE 8 (2): e56255. doi:10.1371/journal.pone.0056255. PMID 23457537. Bibcode: 2013PLoSO...856255D. 
  123. ↑ Hallam, A. (4 April 1996). "Recovery of the marine fauna in Europe after the end-Triassic and Early Toarcian mass Extinctions". Geological Society, London, Special Publications 102 (1): 231–236. doi:10.1144/GSL.SP.1996.001.01.16. Bibcode: 1996GSLSP.102..231H. https://www.lyellcollection.org/doi/abs/10.1144/GSL.SP.1996.001.01.16. Retrieved 14 May 2023. 
  124. ↑ Maxwell, Erin E.; Vincent, Peggy (2015-11-06). "Effects of the early Toarcian Oceanic Anoxic Event on ichthyosaur body size and faunal composition in the Southwest German Basin". Paleobiology 42 (1): 117–126. doi:10.1017/pab.2015.34. ISSN 0094-8373. http://dx.doi.org/10.1017/pab.2015.34. 
  125. ↑ Reolid, Matias; Ruebsam, Wolfgang; Benton, Michael James (22 December 2022). "Dinosaur extinctions related to the Jenkyns Event (early Toarcian, Jurassic)". Spanish Journal of Paleontology 37 (2): 123–140. doi:10.7203/sjp.25683. https://revistas.uv.es/index.php/sjpalaeontology/article/view/25683. Retrieved 2 April 2023. 
  126. ↑ Pol, D.; Ramezani, J.; Gomez, K.; Carballido, J. L.; Carabajal, A. Paulina; Rauhut, O. W. M.; Escapa, I. H.; Cúneo, N. R. (25 November 2020). "Extinction of herbivorous dinosaurs linked to Early Jurassic global warming event" (in en). Proceedings of the Royal Society B: Biological Sciences 287 (1939): 20202310. doi:10.1098/rspb.2020.2310. ISSN 0962-8452. PMID 33203331. PMC 7739499. https://royalsocietypublishing.org/doi/10.1098/rspb.2020.2310. Retrieved 30 December 2023. 
  127. ↑ Jin, Xin; Zhang, Fei; Baranyi, Viktória; Kemp, David B.; Feng, Xinbin; Grasby, Stephen E.; Sun, Guangyi; Shi, Zhiqiang et al. (15 November 2022). "Early Jurassic massive release of terrestrial mercury linked to floral crisis". Earth and Planetary Science Letters 598: 117842. doi:10.1016/j.epsl.2022.117842. Bibcode: 2022E&PSL.59817842J. https://www.sciencedirect.com/science/article/abs/pii/S0012821X22004782. Retrieved 14 June 2023. 
  128. ↑ Baranyi, Viktória; Jin, Xin; Dal Corso, Jacopo; Shi, Zhiqiang; Grasby, Stephen E.; Kemp, David B. (8 May 2023). "Collapse of terrestrial ecosystems linked to heavy metal poisoning during the Toarcian oceanic anoxic event". Geology 51 (7): 652–656. doi:10.1130/G51037.1. Bibcode: 2023Geo....51..652B. https://pubs.geoscienceworld.org/gsa/geology/article-abstract/doi/10.1130/G51037.1/623294/Collapse-of-terrestrial-ecosystems-linked-to-heavy. Retrieved 14 June 2023. 
  129. ↑ Sinha, Sinjini; Muscente, A. D.; Schiffbauer, James D.; Williams, Matt; Schweigert, Günter; Martindale, Rowan C. (16 December 2021). "Global controls on phosphatization of fossils during the Toarcian Oceanic Anoxic Event". Scientific Reports 11 (1): 24087. doi:10.1038/s41598-021-03482-7. PMID 34916533. PMC 8677819. Bibcode: 2021NatSR..1124087S. https://www.researchgate.net/publication/357093726. Retrieved 17 July 2023. 
  130. ↑ Lézin, Carine; Andreu, Bernard; Pellenard, Pierre; Buchez, Jean-Luc; Emmanuel, Laurent; Fauré, Philippe; Landrein, Philippe (11 March 2013). "Geochemical disturbance and paleoenvironmental changes during the Early Toarcian in NW Europe". Chemical Geology 341: 1–15. doi:10.1016/j.chemgeo.2013.01.003. Bibcode: 2013ChGeo.341....1L. https://www.sciencedirect.com/science/article/abs/pii/S0009254113000314. Retrieved 17 December 2022. 
  131. ↑ Fernández-Martínez, Javier; Rodríguez-Tovar, Francisco J.; Piñuela, Laura; Martínez-Ruiz, Francisca; García-Ramos, José C. (15 June 2021). "Bottom- and pore-water oxygenation during the early Toarcian Oceanic Anoxic Event (T-OAE) in the Asturian Basin (N Spain): Ichnological information to improve facies analysis". Sedimentary Geology 419: 105909. doi:10.1016/j.sedgeo.2021.105909. Bibcode: 2021SedG..41905909F. https://www.sciencedirect.com/science/article/abs/pii/S0037073821000610. Retrieved 2 April 2023. 
  132. ↑ Jones, Charles E.; Jenkyns, Hugh C. (February 2001). "Seawater Strontium Isotopes, Oceanic Anoxic Events, and Seafloor Hydrothermal Activity in the Jurassic and Cretaceous". American Journal of Science 301 (2): 112–149. doi:10.2475/ajs.301.2.112. Bibcode: 2001AmJS..301..112J. https://www.ajsonline.org/content/301/2/112.short. Retrieved 8 April 2023. 
  133. ↑ Yi, Fan; Yi, Haisheng; Xia, Guoqing; Wu, Chihua; Li, Gaojie; Cai, Zhanhu; Li, Na (November 2021). "Factors controlling the organic matter accumulation across the Pliensbachian-Toarcian transition in the Qiangtang Basin, Tibetan Plateau". Marine and Petroleum Geology 133: 105304. doi:10.1016/j.marpetgeo.2021.105304. Bibcode: 2021MarPG.13305304Y. https://www.sciencedirect.com/science/article/abs/pii/S0264817221004074. Retrieved 8 January 2023. 
  134. ↑ Qiu, Zhen; He, Jianglin (1 July 2022). "Depositional environment changes and organic matter accumulation of Pliensbachian-Toarcian lacustrine shales in the Sichuan basin, SW China". Journal of Asian Earth Sciences 232. doi:10.1016/j.jseaes.2021.105035. https://www.sciencedirect.com/science/article/abs/pii/S1367912021003734. Retrieved 5 August 2023. 
  135. ↑ Xu, Weimu; Ruhl, Micha; Jenkyns, Hugh C.; Leng, Melanie J.; Huggett, Jennifer M.; Minisini, Daniel; Ullmann, Clemens V.; Riding, James B. et al. (15 February 2018). "Evolution of the Toarcian (Early Jurassic) carbon-cycle and global climatic controls on local sedimentary processes (Cardigan Bay Basin, UK)". Earth and Planetary Science Letters 484: 396–411. doi:10.1016/j.epsl.2017.12.037. ISSN 0012-821X. https://www.sciencedirect.com/science/article/pii/S0012821X17307495. Retrieved 26 November 2023. 
  136. ↑ Dera, Guillaume; Pellenard, Pierre; Neige, Pascal; Deconinck, Jean-François; Pucéat, Emmanuelle; Dommergues, Jean-Louis (1 January 2009). "Distribution of clay minerals in Early Jurassic Peritethyan seas: Palaeoclimatic significance inferred from multiproxy comparisons". Palaeogeography, Palaeoclimatology, Palaeoecology 271 (1–2): 39–51. doi:10.1016/j.palaeo.2008.09.010. Bibcode: 2009PPP...271...39D. https://www.sciencedirect.com/science/article/abs/pii/S0031018208005269. Retrieved 17 July 2023. 
  137. ↑ Müller, Tamás; Price, Gregory D.; Bajnai, Dávid; Nyerges, Anita; Kesjár, Dóra; Raucsik, Béla; Varga, Andrea; Judik, Katalin et al. (7 October 2016). "New multiproxy record of the Jenkyns Event (also known as the Toarcian Oceanic Anoxic Event) from the Mecsek Mountains (Hungary): Differences, duration and drivers". Sedimentology 64 (1): 66–86. doi:10.1111/sed.12332. https://onlinelibrary.wiley.com/doi/abs/10.1111/sed.12332. Retrieved 8 April 2023. 
  138. ↑ Mattioli, Emanuela; Pittet, Bernard; Suan, Guillaume; Mailliot, Samuel (23 July 2008). "Calcareous nannoplankton changes across the early Toarcian oceanic anoxic event in the western Tethys". Paleoceanography and Paleoclimatology 23 (3): 1–17. doi:10.1029/2007PA001435. Bibcode: 2008PalOc..23.3208M. 
  139. ↑ Liu, Jinchao; Cao, Jian; He, Tianchen; Liang, Feng; Pu, Jing; Wang, Yan (August 2022). "Lacustrine redox variations in the Toarcian Sichuan Basin across the Jenkyns Event". Global and Planetary Change 215: 103860. doi:10.1016/j.gloplacha.2022.103860. Bibcode: 2022GPC...21503860L. https://www.sciencedirect.com/science/article/abs/pii/S0921818122001278. Retrieved 17 December 2022. 
  140. ↑ Xu, Weimu; Weijers, Johan W. H.; Ruhl, Micha; Idiz, Erdem F.; Jenkyns, Hugh C.; Riding, James B.; Gorbanenko, Olga; Hesselbo, Stephen P. (2 July 2021). "Molecular and petrographical evidence for lacustrine environmental and biotic change in the palaeo-Sichuan mega-lake (China) during the Toarcian Oceanic Anoxic Event". Geological Society Special Publications 514 (1): 335–357. doi:10.1144/SP514-2021-2. Bibcode: 2021GSLSP.514..335X. https://www.lyellcollection.org/doi/abs/10.1144/SP514-2021-2. Retrieved 2 April 2023. 
  141. ↑ 141.0 141.1 Xu, Weimu; Ruhl, Micha; Jenkyns, Hugh C.; Hesselbo, Stephen P.; Riding, James B.; Selby, David; Naafs, B. David A.; Weijers, Johan W. H. et al. (February 2017). "Carbon sequestration in an expanded lake system during the Toarcian oceanic anoxic event" (in en). Nature Geoscience 10 (2): 129–134. doi:10.1038/ngeo2871. ISSN 1752-0894. Bibcode: 2017NatGe..10..129X. http://www.nature.com/articles/ngeo2871. 
  142. ↑ Liu, Renping; Hu, Guang; Cao, Jian; Yang, Ruofei; Liao, Zhiwei; Hu, Chaowei; Pang, Qian; Pang, Peng (September 2022). "Enhanced hydrological cycling and continental weathering during the Jenkyns Event in a lake system in the Sichuan Basin, China". Global and Planetary Change 216. doi:10.1016/j.gloplacha.2022.103915. https://www.sciencedirect.com/science/article/abs/pii/S0921818122001825. Retrieved 16 August 2023. 



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