Toarcian Oceanic Anoxic Event

Last updated

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]

Contents

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] Occurring during a broader, gradual positive carbon isotope excursion as measured by δ13C values, the TOAE is preceded by a global negative δ13C excursion recognised in fossil wood, organic carbon, and carbonate carbon in the tenuicostatum ammonite zone of northwestern Europe, [41] with this negative δ13C shift being the result of volcanic discharge of light carbon. [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, [42] though its occurrence in areas like Greece has been cited as evidence of its global nature. [43] The negative δ13C shift is also known from the Arabian Peninsula, [44] the Ordos Basin, [45] and the Neuquén Basin. [46] 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] Although the PTo-E is not associated with a decrease in δ13C analogous to the TOAE's, volcanism is nonetheless believed to have been responsible for its onset as well, with the carbon injection most likely having an isotopically heavy, mantle-derived origin. [47] 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. [48] 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. [49] 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, [50] [51] [52] although some researchers attribute these elevated mercury levels to increased terrigenous flux. [53] 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. [54] 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. [55]

The large igneous province also intruded into coal seams, releasing even more carbon dioxide and methane than it otherwise would have. [56] [57] [16] Magmatic sills are also known to have intruded into shales rich in organic carbon, causing additional venting of carbon dioxide into the atmosphere. [58] Carbon release via metamorphic heating of coal has been criticised as a major driver of the environmental perturbation, however, on the basis that coal transects themselves do not show the δ13C excursions that would be expected if significant quantities of thermogenic methane were released, suggesting that much of the degassed emissions were either condensed as pyrolytic carbon or trapped as coalbed methane. [59]

In addition, possible associated release of deep sea methane clathrates has been potentially implicated as yet another cause of global warming. [60] [61] [62] 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. [63] [26] [64] 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, [65] that carbon isotope ratios in belemnites and bulk carbonates are incongruent with the isotopic signature expected from a massive release of methane clathrates, [66] that much of the methane released from ocean sediments was rapidly sequestered, buffering its ability to act as a major positive feedback, [67] and that methane clathrate dissociation occurred too late to have had an appreciable causal impact on the extinction event. [68] Hypothetical release of methane clathrates extremely depleted in heavy carbon isotopes has furthermore been considered unnecessary as an explanation for the carbon cycle disruption. [69]

It has also been hypothesised that the release of cryospheric methane trapped in permafrost amplified the warming and its detrimental effects on marine life. [70] [71] Obliquity-paced carbon isotope excursions have been interpreted as some researchers as reflective of permafrost decline and consequent greenhouse gas release. [72] [73]

The TOAE is believed to be the second largest anoxic event of the last 300 Ma, [74] and possibly the largest of the Phanerozoic. [10] A positive δ13C excursion, likely resulting from the mass burial of organic carbon during the anoxic event, is known from the falciferum ammonite zone, chemostratigraphically identifying the TOAE. [75] Large igneous province resulted in increased silicate weathering and an acceleration of the hydrological cycle, [76] [77] as shown by a increased amount of terrestrially derived organic matter found in sedimentary rocks of marine origin during the TOAE. [78] [79] Concentrations of phosphorus, magnesium, and manganese rose in the oceans. [80] A -0.5% excursion in δ44/40Ca provides further evidence of increased continental weathering. [81] Osmium isotope ratios confirm further still a major increase in weathering. [82] The enhanced continental weathering in turn led to increased eutrophication that helped drive the anoxic event in the oceans. [14] [83] [84] 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] Rising sea levels contributed to ocean deoxygenation; [85] as rising sea levels inundated low-lying lands, organic plant matter was transported outwards into the ocean. [86] 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. [87] 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. [88] Stratification also occurred due to the freshening of surface water caused by an enhanced water cycle. [89] [90] Rising seawater temperatures amidst a transition from icehouse to greenhouse conditions further retarded ocean circulation, aiding the establishment of anoxic conditions. [91] 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] 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. [92] 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. [93] [94]

Euxinia occurred in the northwestern Tethys Ocean during the TOAE, as shown by a positive δ34S excursion in carbonate-associated sulphate occurs synchronously with the positive δ13C excursion in carbonate carbon during the falciferum ammonite zone. This positive δ34S 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. [95] Similar positive δ34S 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 δ34S excursion during the PTo-E. [96] Euxinia is further evidenced by enhanced pyrite burial in Zázrivá, Slovakia, [97] enhanced molybdenum burial totalling about 41 Gt of molybdenum, [98] and δ98/95Mo excursions observed in sites in the Cleveland, West Netherlands, and South German Basins. [99] 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. [100] 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. [101] 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. [102] In northeastern Panthalassa, in what is now British Columbia, euxinia dominated anoxic bottom waters. [103]

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. [104] [105] [106] 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. [107]

The extreme and rapid global warming at the start of the Toarcian promoted intensification of tropical storms across the globe. [108] [109]

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. [110] Brachiopods were particularly severely hit, [111] [2] [112] with the TOAE representing one of the most dire crises in their evolutionary history. [113] Brachiopod taxa of large size declined significantly in abundance. [114] 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. [115] The species S. bouchardi is known to have been a pioneer species that colonised areas denuded of brachiopods in the northwestern Tethyan region. [116] Ostracods also suffered a major diversity loss, [117] [118] 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. [118] 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, [119] while in the Cleveland Basin, the inoceramid Pseudomytiloides dubius experienced the Lilliput effect. [120] Ammonoids, having already experienced a major morphological bottleneck thanks to the Gibbosus Event, [121] about a million years before the Toarcian extinction, suffered further losses in the Early Toarcian diversity collapse. [122] Belemnite richness in the northwestern Tethys dropped during the PTo-E but slightly increased across the TOAE. [123] 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. [123] The Toarcian extinction was unbelievably catastrophic for corals; 90.9% of all Tethyan coral species and 49% of all genera were wiped out. [124] 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. [125] Other affected invertebrate groups included echinoderms, [126] radiolarians, [127] dinoflagellates, [126] and foraminifera. [128] [129] [117] Trace fossils, an indicator of bioturbation and ecological diversity, became highly undiverse following the TOAE. [130]

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. [131] Evidence from the Cleveland Basin suggests it took ~7 Myr for the marine benthos to recover, on par with the Permian-Triassic extinction event. [132] [133] 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. [134]

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. [135]

Terrestrial animals

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. [136] 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. [137] Megalosaurids experienced a diversification event in the latter part of the Toarcian that was possibly a post-extinction radiation that filled niches vacated by the mass death of the Early Toarcian extinction. [138] Insects may have experienced blooms as fish moved en masse to surface waters to escape anoxia and then died in droves due to limited resources. [139]

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. [83] 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. [140] 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. [141]

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. [142]

As is common during anoxic events, black shale deposition was widespread during the deoxygenation events of the Toarcian. [143] [18] [144] Toarcian anoxia was responsible for the deposition of commercially extracted oil shales, [145] particularly in China. [146] [147]

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. [148]

Additionally, the Toarcian was punctuated by intervals of extensive kaolinite enrichment. [149] 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. [150] Likewise, illitic/smectitic clays were also common during this hyperthermal perturbation. [151]

Palaeogeographic changes

The Intertropical Convergence Zone (ITCZ) 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. [152]

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. [153]

The enhanced hydrological cycle during early Toarcian warming caused lakes to grow in size. [45] During the anoxic event, the Sichuan Basin was transformed into a giant lake, [154] [155] which was believed to be approximately thrice as large as modern-day Lake Superior. [156] Lacustrine sediments deposited as a result of this lake's existence are represented by the Da’anzhai Member of the Ziliujing Formation. [157] 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. [156]

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. [61] 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. [109]

See also

Related Research Articles

<span class="mw-page-title-main">Extinction event</span> Widespread and rapid decrease in the biodiversity on Earth

An extinction event is a widespread and rapid decrease in the biodiversity on Earth. Such an event is identified by a sharp fall in the diversity and abundance of multicellular organisms. It occurs when the rate of extinction increases with respect to the background extinction rate and the rate of speciation. Estimates of the number of major mass extinctions in the last 540 million years range from as few as five to more than twenty. These differences stem from disagreement as to what constitutes a "major" extinction event, and the data chosen to measure past diversity.

<span class="mw-page-title-main">Jurassic</span> Second period of the Mesozoic Era 201-145 million years ago

The Jurassic is a geologic period and stratigraphic system that spanned from the end of the Triassic Period 201.4 million years ago (Mya) to the beginning of the Cretaceous Period, approximately 145 Mya. The Jurassic constitutes the middle period of the Mesozoic Era as well as the eighth period of the Phanerozoic Eon and is named after the Jura Mountains, where limestone strata from the period were first identified.

<span class="mw-page-title-main">Permian–Triassic extinction event</span> Earths most severe extinction event

Approximately 251.9 million years ago, the Permian–Triassicextinction event forms the boundary between the Permian and Triassic geologic periods, and with them the Paleozoic and Mesozoic eras. It is Earth's most severe known extinction event, with the extinction of 57% of biological families, 83% of genera, 81% of marine species and 70% of terrestrial vertebrate species. It is also the greatest known mass extinction of insects. It is the greatest of the "Big Five" mass extinctions of the Phanerozoic. There is evidence for one to three distinct pulses, or phases, of extinction.

<span class="mw-page-title-main">Triassic–Jurassic extinction event</span> Mass extinction ending the Triassic period

The Triassic–Jurassic (Tr-J) extinction event (TJME), often called the end-Triassic extinction, marks the boundary between the Triassic and Jurassic periods, 201.4 million years ago. It is one of five major extinction events, profoundly affecting life on land and in the oceans. In the seas, about 23–34% of marine genera disappeared. On land, all archosauromorph reptiles other than crocodylomorphs, dinosaurs, and pterosaurs became extinct; some of the groups which died out were previously abundant, such as aetosaurs, phytosaurs, and rauisuchids. Plants, crocodylomorphs, dinosaurs, pterosaurs and mammals were left largely untouched, allowing the dinosaurs, pterosaurs, and crocodylomorphs to become the dominant land animals for the next 135 million years.

<span class="mw-page-title-main">Paleocene–Eocene Thermal Maximum</span> Global warming about 55 million years ago

The Paleocene–Eocene thermal maximum (PETM), alternatively ”Eocene thermal maximum 1 (ETM1)“ and formerly known as the "Initial Eocene" or “Late Paleocene thermal maximum", was a geologically brief time interval characterized by a 5–8 °C global average temperature rise and massive input of carbon into the ocean and atmosphere. The event began, now formally codified, at the precise time boundary between the Paleocene and Eocene geological epochs. The exact age and duration of the PETM remain uncertain, but it occurred around 55.8 million years ago (Ma) and lasted about 200 thousand years (Ka).

<span class="mw-page-title-main">Late Ordovician mass extinction</span> Extinction event around 444 million years ago

The Late Ordovician mass extinction (LOME), sometimes known as the end-Ordovician mass extinction or the Ordovician-Silurian extinction, is the first of the "big five" major mass extinction events in Earth's history, occurring roughly 445 million years ago (Ma). It is often considered to be the second-largest known extinction event just behind the end-Permian mass extinction, in terms of the percentage of genera that became extinct. Extinction was global during this interval, eliminating 49–60% of marine genera and nearly 85% of marine species. Under most tabulations, only the Permian-Triassic mass extinction exceeds the Late Ordovician mass extinction in biodiversity loss. The extinction event abruptly affected all major taxonomic groups and caused the disappearance of one third of all brachiopod and bryozoan families, as well as numerous groups of conodonts, trilobites, echinoderms, corals, bivalves, and graptolites. Despite its taxonomic severity, the Late Ordovician mass extinction did not produce major changes to ecosystem structures compared to other mass extinctions, nor did it lead to any particular morphological innovations. Diversity gradually recovered to pre-extinction levels over the first 5 million years of the Silurian period.

<span class="mw-page-title-main">Late Devonian extinction</span> One of the five most severe extinction events in the history of the Earths biota

The Late Devonian extinction consisted of several extinction events in the Late Devonian Epoch, which collectively represent one of the five largest mass extinction events in the history of life on Earth. The term primarily refers to a major extinction, the Kellwasser event, also known as the Frasnian-Famennian extinction, which occurred around 372 million years ago, at the boundary between the Frasnian age and the Famennian age, the last age in the Devonian Period. Overall, 19% of all families and 50% of all genera became extinct. A second mass extinction called the Hangenberg event, also known as the end-Devonian extinction, occurred 359 million years ago, bringing an end to the Famennian and Devonian, as the world transitioned into the Carboniferous Period.

An anoxic event describes a period wherein large expanses of Earth's oceans were depleted of dissolved oxygen (O2), creating toxic, euxinic (anoxic and sulfidic) waters. Although anoxic events have not happened for millions of years, the geologic record shows that they happened many times in the past. Anoxic events coincided with several mass extinctions and may have contributed to them. These mass extinctions include some that geobiologists use as time markers in biostratigraphic dating. On the other hand, there are widespread, various black-shale beds from the mid-Cretaceous which indicate anoxic events but are not associated with mass extinctions. Many geologists believe oceanic anoxic events are strongly linked to the slowing of ocean circulation, climatic warming, and elevated levels of greenhouse gases. Researchers have proposed enhanced volcanism (the release of CO2) as the "central external trigger for euxinia."

The Toarcian is, in the ICS' geologic timescale, an age and stage in the Early or Lower Jurassic. It spans the time between 184.2 Ma and 174.7 ±0.8 Ma. It follows the Pliensbachian and is followed by the Aalenian.

<span class="mw-page-title-main">Aptian</span> Fifth age of the Early Cretaceous

The Aptian is an age in the geologic timescale or a stage in the stratigraphic column. It is a subdivision of the Early or Lower Cretaceous Epoch or Series and encompasses the time from 121.4 ± 1.0 Ma to 113.0 ± 1.0 Ma, approximately. The Aptian succeeds the Barremian and precedes the Albian, all part of the Lower/Early Cretaceous.

The Ziliujing Formation is a geological formation in China, It is Early Jurassic in age. It is part of the stratigraphy of the Sichuan Basin. The dinosaur Gongxianosaurus and indeterminate theropod material are known from the Dongyuemiao Member of the formation, as well as dinosaur footprints, Zizhongosaurus and indeterminate prosauropods from the Da'anzhai Member. The basal sauropod Sanpasaurus is known from the Maanshan Member. An possible unnamed stegosaur and the pliosauroid plesiosaur Sinopliosaurus are also known from this formation but they were found an indeterminate member. An unnamed teleosaurid known from a complete skull has also been found in the formation, pending a formal description. The deposition environment during the Da'anzhai Member in the lower Toarcian is thought to have been that of a giant freshwater lake encompassing the whole of the Sichuan basin, around 3 times larger than Lake Superior, coeval with the Toarcian Oceanic Anoxic Event around 183 Ma. The Sinemurian-Pliensbachian boundary event has been recorded on the top of the Dongyuemiao Member, while lower parts of this member are of Earliest Sinemurian age.

The Great Ordovician Biodiversification Event (GOBE), was an evolutionary radiation of animal life throughout the Ordovician period, 40 million years after the Cambrian explosion, whereby the distinctive Cambrian fauna fizzled out to be replaced with a Paleozoic fauna rich in suspension feeder and pelagic animals.

<span class="mw-page-title-main">Posidonia Shale</span> Early Jurassic geological formation of south-western Germany

The Posidonia Shale geologically known as the Sachrang Formation, is an Early Jurassic geological formation of southwestern and northeast Germany, northern Switzerland, northwestern Austria, southern Luxembourg and the Netherlands, including exceptionally well-preserved complete skeletons of fossil marine fish and reptiles.

The Cenomanian-Turonian boundary event, also known as the Cenomanian-Turonian extinction, Cenomanian-Turonian Oceanic Anoxic Event, and referred to also as the Bonarelli Event or Level, was an anoxic extinction event in the Cretaceous period. The Cenomanian-Turonian oceanic anoxic event is considered to be the most recent truly global oceanic anoxic event in Earth's geologic history. There was a large carbon cycle disturbance during this time period, signified by a large positive carbon isotope excursion. However, apart from the carbon cycle disturbance, there were also large disturbances in the ocean's nitrogen, oxygen, phosphorus, sulphur, and iron cycles.

Euxinia or euxinic conditions occur when water is both anoxic and sulfidic. This means that there is no oxygen (O2) and a raised level of free hydrogen sulfide (H2S). Euxinic bodies of water are frequently strongly stratified; have an oxic, highly productive, thin surface layer; and have anoxic, sulfidic bottom water. The word "euxinia" is derived from the Greek name for the Black Sea (Εὔξεινος Πόντος (Euxeinos Pontos)) which translates to "hospitable sea". Euxinic deep water is a key component of the Canfield ocean, a model of oceans during part of the Proterozoic eon (a part specifically known as the Boring Billion) proposed by Donald Canfield, an American geologist, in 1998. There is still debate within the scientific community on both the duration and frequency of euxinic conditions in the ancient oceans. Euxinia is relatively rare in modern bodies of water, but does still happen in places like the Black Sea and certain fjords.

The Calcare di Sogno is a geological formation in Italy, dated to roughly between 182-169 million years ago and covering the Lower Toarcian-Late Bajocian stagess of the Jurassic Period in the Mesozoic Era. Thallatosuchian remains are known from the formation, as well fishes and other taxa.

<span class="mw-page-title-main">Sorthat Formation</span> Geologic formation in Bornholm, Denmark

The Sorthat Formation is a geologic formation on the island of Bornholm, Denmark and in the Rønne Graben in the Baltic Sea. It is of Latest Pliensbachian to Late Toarcian age. Plant fossils have been recovered from the formation, along with several traces of invertebrate animals. The Sorthat Formation is overlain by fluvial to lacustrine gravels, along with sands, clay and in some places coal beds that are part of the Aalenian-Bathonian Bagå Formation. Until 2003, the Sorthat Formation was included as the lowermost part of the Bagå Formation, recovering the latest Pliensbachian to lower Aalenian boundary. The Sorthat strata reflect a mostly marginally deltaic to marine unit. Large streams fluctuated to the east, where a large river system was established at the start of the Toarcian. In the northwest, local volcanism that started in the lower Pliensbachian extended along the North Sea, mostly from southern Sweden. At this time, the Central Skåne Volcanic Province and the Egersund Basin expelled most of their material, with influences on the local tectonics. The Egersund Basin has abundant fresh porphyritic nephelinite lavas and dykes of lower Jurassic age, with a composition nearly identical to those found in the clay pits. That indicates the transport of strata from the continental margin by large fluvial channels of the Sorthat and the connected Röddinge Formation that ended in the sea deposits of the Ciechocinek Formation green series.

The Selli Event, also known as OAE1a, was an oceanic anoxic event (OAE) of global scale that occurred during the Aptian stage of the Early Cretaceous, about 120.5 million years ago (Ma). The OAE is associated with large igneous province volcanism and an extinction event of marine organisms driven by global warming, ocean acidification, and anoxia.

The Breistroffer Event (OAE1d) was an oceanic anoxic event (OAE) that occurred during the middle Cretaceous period, specifically in the latest Albian, around 101 million years ago (Ma).

The Paquier Event (OAE1b) was an oceanic anoxic event (OAE) that occurred around 111 million years ago (Ma), in the Albian geologic stage, during a climatic interval of Earth's history known as the Middle Cretaceous Hothouse (MKH).

References

  1. 1 2 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. Bibcode:2000JGSoc.157...55A. doi:10.1144/jgs.157.1.55. S2CID   129652851 . Retrieved 14 May 2023.
  2. 1 2 Caruthers, Andrew H.; Smith, Paul L.; Gröcke, Darren R. (September 2013). "The Pliensbachian–Toarcian (Early Jurassic) extinction, a global multi-phased event". Palaeogeography, Palaeoclimatology, Palaeoecology . 386: 104–118. Bibcode:2013PPP...386..104C. doi:10.1016/j.palaeo.2013.05.010.
  3. 1 2 3 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. Bibcode:2016CliPa..12.1199G. doi: 10.5194/cp-12-1199-2016 . hdl: 10261/133460 . Retrieved 14 May 2023.
  4. 1 2 3 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. Bibcode:2008PalOc..23.1202S. doi: 10.1029/2007PA001459 . S2CID   129137256.
  5. 1 2 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. Bibcode:2022ESRv..23104086K. doi:10.1016/j.earscirev.2022.104086. S2CID   249693286 . Retrieved 3 January 2023.
  6. 1 2 Reolid, Matías; Mattioli, Emanuela; Duarte, Luís V.; Ruebsam, Wolfgang (2021-09-22). "The Toarcian Oceanic Anoxic Event: where do we stand?". Geological Society, London, Special Publications. 514 (1): 1–11. Bibcode:2021GSLSP.514....1R. doi:10.1144/SP514-2021-74. ISSN   0305-8719. S2CID   238683028.
  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)". Episodes . 43 (2): 833–844. doi: 10.18814/epiiugs/2020/020051 . ISSN   0705-3797. S2CID   216195656.
  8. 1 2 3 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. Bibcode:2014GPC...117...64K. doi:10.1016/j.gloplacha.2014.03.008 . Retrieved 20 January 2023.
  9. 1 2 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. Bibcode:2022GPC...21203782K. doi:10.1016/j.gloplacha.2022.103782. S2CID   247424412 . Retrieved 1 January 2023.
  10. 1 2 3 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 . PMC   4104856 . PMID   24982187.
  11. 1 2 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. Bibcode:2021ESRv..21503503S. doi:10.1016/j.earscirev.2021.103503. ISSN   0012-8252. S2CID   233579194. Archived from the original on 8 January 2021. Retrieved 17 July 2023. Alt URL
  12. 1 2 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. Bibcode:2000Geo....28..747P. doi:10.1130/0091-7613(2000)28<747:SBEJEO>2.0.CO;2 . Retrieved 17 April 2023.
  13. 1 2 Müller, Tamás; Jurikova, Hana; Gutjahr, Marcus; Tomašových, Adam; Schlögl, Jan; Liebetrau, Volker; Duarte, Luís v.; Milovský, Rastislav; Suan, Guillaume; Mattioli, Emanuela; Pittet, Bernard (2020-12-01). "Ocean acidification during the early Toarcian extinction event: Evidence from boron isotopes in brachiopods". Geology . 48 (12): 1184–1188. Bibcode:2020Geo....48.1184M. doi: 10.1130/G47781.1 . hdl: 10023/20595 . ISSN   0091-7613.
  14. 1 2 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. Bibcode:2022JAESc.23705344X. doi:10.1016/j.jseaes.2022.105344. S2CID   250976430 . Retrieved 8 January 2023.
  15. 1 2 3 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. Bibcode:2022ESRv..23404196R. doi: 10.1016/j.earscirev.2022.104196 . S2CID   252608726.
  16. 1 2 3 4 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". Earth and Planetary Science Letters . 459: 118–126. Bibcode:2017E&PSL.459..118T. doi: 10.1016/j.epsl.2016.11.021 .
  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. Bibcode:2019PPP...525...57R. doi:10.1016/j.palaeo.2019.04.009. hdl: 11336/128130 . S2CID   146525666 . Retrieved 23 November 2022.
  18. 1 2 Suan, Guillaume; Rulleau, Louis; Mattioli, Emanuela; Suchéras-Marx, Baptiste; Rouselle, Bruno; Pittet, Bernard; Vincent, Peggy; Martin, Jeremy E.; Léna, Alex; Spangenberg, Jorge E.; Föllmi, Karl B. (7 February 2013). "Palaeoenvironmental significance of Toarcian black shales and event deposits from southern Beaujolais, France". Geological Magazine . 150 (4): 728–742. Bibcode:2013GeoM..150..728S. doi:10.1017/S0016756812000970. S2CID   53574804 . 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 . Retrieved 14 June 2023.
  20. 1 2 3 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. Bibcode:2013PPP...387...40A. doi:10.1016/j.palaeo.2013.07.004 . 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. S2CID   129648354 . 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.; Storm, Marisa; Riccardi, Alberto C.; Hesselbo, Stephen P. (23 March 2022). "New age constraints on the Lower Jurassic Pliensbachian–Toarcian Boundary at Chacay Melehue (Neuquén Basin, Argentina)". Scientific Reports . 12 (1): 4975. Bibcode:2022NatSR..12.4975A. doi:10.1038/s41598-022-07886-x. PMC   8942990 . PMID   35322043.
  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. Bibcode:2019GPC...175..113B. doi:10.1016/j.gloplacha.2019.02.005. ISSN   0921-8181. S2CID   134411583 . Retrieved 26 November 2023.
  24. 1 2 3 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. Bibcode:2003E&PSL.212..307B. doi:10.1016/S0012-821X(03)00278-4 . 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. Bibcode:2000E&PSL.179..269M. doi:10.1016/S0012-821X(00)00111-4 . Retrieved 5 August 2023.
  26. 1 2 3 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. Bibcode:2009Sedim..56.1307S. doi:10.1111/j.1365-3091.2008.01035.x. S2CID   140543701 . Retrieved 8 April 2023.
  27. 1 2 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. Bibcode:2020ESRv..20803254K. doi:10.1016/j.earscirev.2020.103254. S2CID   225669068 . 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. Bibcode:2020GPC...19503351R. doi: 10.1016/j.gloplacha.2020.103351 . S2CID   225109000.
  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. Bibcode:2021PPP...57710562R. doi: 10.1016/j.palaeo.2021.110562 .
  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): 10. Bibcode:2023Faci...69...10M. 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. S2CID   245569085 . Retrieved 16 August 2023.
  32. ↑ Suan, Guillaume; Mattioli, Emanuela; Pittet, Bernard; Lécuyer, Christophe; Suchéras-Marx, Baptiste; Duarte, Luís Vítor; Philippe, Marc; Reggiani, Letizia; Martineau, François (20 February 2010). "Secular environmental precursors to Early Toarcian (Jurassic) extreme climate changes". Earth and Planetary Science Letters . 290 (3–4): 448–458. Bibcode:2010E&PSL.290..448S. doi:10.1016/j.epsl.2009.12.047. hdl: 10316/20069 . 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. Bibcode:2020NatSR..10..117R. doi:10.1038/s41598-019-56710-6. PMC   6954244 . PMID   31924807.
  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. Bibcode:2020PLoSO..1542331P. doi: 10.1371/journal.pone.0242331 . PMC   7725388 . PMID   33296368.
  35. ↑ Font, Eric; Duarte, Luís Vítor; Dekkers, Mark J.; Remazeilles, Celine; Egli, Ramon; Spangenberg, Jorge E.; Fantasia, Alicia; Ribeiro, Joana; Gomes, Elsa; Mirão, José; Adatte, Thierry (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. Bibcode:2022NatSR..12.4342F. doi:10.1038/s41598-022-08269-y. PMC   8921222 . PMID   35288615.
  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. Bibcode:2004JGSoc.161..547R. doi:10.1144/0016-764903-181. S2CID   129916780 . 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. Bibcode:2012E&PSL.325....1S. doi:10.1016/j.epsl.2012.01.015 . 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. Bibcode:2015E&PSL.415...90B. doi:10.1016/j.epsl.2015.01.037 . 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. Bibcode:2016E&PSL.434..349C. doi:10.1016/j.epsl.2015.07.010 . 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)". Journal of Geophysical Research . 116 (B7): 1–27. Bibcode:2011JGRB..116.7403M. doi: 10.1029/2011JB008210 . ISSN   0148-0227.
  41. ↑ 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. Bibcode:2007E&PSL.253..455H. doi:10.1016/j.epsl.2006.11.009. hdl: 10316/3934 . Retrieved 11 January 2023.
  42. ↑ 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. Bibcode:2015GPC...126...62N. doi:10.1016/j.gloplacha.2015.01.007 . Retrieved 8 January 2023.
  43. ↑ 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. Bibcode:2011GeoM..148..619K. doi:10.1017/S0016756811000082. S2CID   30165407 . Retrieved 13 March 2023.
  44. ↑ 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. Bibcode:2022NatSR..1218124A. doi:10.1038/s41598-022-21716-0. PMC   9613744 . PMID   36302804.
  45. 1 2 Jin, Xin; Shi, Zhiqiang; Baranyi, Viktória; Kemp, David B.; Han, Zhong; Luo, Genming; Hu, Jianfang; He, Feng; Chen, Lan; Preto, Nereo (October 2020). "The Jenkyns Event (early Toarcian OAE) in the Ordos Basin, North China". Global and Planetary Change . 193: 103273. Bibcode:2020GPC...19303273J. doi:10.1016/j.gloplacha.2020.103273. S2CID   224876498 . Retrieved 14 May 2023.
  46. ↑ 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. Bibcode:2010E&PSL.297..633M. doi:10.1016/j.epsl.2010.07.017. hdl: 11336/69031 . Retrieved 14 May 2023.
  47. ↑ Bodin, Stephane; Krencker, Francois-Nicolas; Kothe, Tim; Hoffmann, Rene; Mattioli, Emanuela; Heimhofer, Ulrich; Kabiri, Lahcen (19 December 2015). "Perturbation of the carbon cycle during the late Pliensbachian -- early Toarcian: New insight from high-resolution carbon isotope records in Morocco". Journal of African Earth Sciences . 116: 89–104. doi:10.1016/j.jafrearsci.2015.12.018 . Retrieved 10 March 2024– via Elsevier Science Direct.
  48. ↑ Martinez, Mathieu; Dera, Guillaume (13 October 2015). "Orbital pacing of carbon fluxes by a ∼9-My eccentricity cycle during the Mesozoic". Proceedings of the National Academy of Sciences of the United States of America . 112 (41): 12604–12609. Bibcode:2015PNAS..11212604M. doi: 10.1073/pnas.1419946112 . ISSN   0027-8424. PMC   4611626 . PMID   26417080.
  49. ↑ 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.; Storm, M. S.; Xu, W. (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. Bibcode:2016Geo....44..759P. doi: 10.1130/G37997.1 . hdl: 10871/22441 . S2CID   22328529.
  50. ↑ Fendley, Isabel M.; Frieling, Joost; Mather, Tamsin A.; Ruhl, Micha; Hesselbo, Stephen P.; Jenkyns, Hugh C. (26 February 2024). "Early Jurassic large igneous province carbon emissions constrained by sedimentary mercury". Nature Geoscience . 17 (3): 241–248. Bibcode:2024NatGe..17..241F. doi: 10.1038/s41561-024-01378-5 . ISSN   1752-0894.
  51. ↑ 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.; Xu, W.; Ruhl, M. (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. Bibcode:2015E&PSL.428..267P. doi:10.1016/j.epsl.2015.06.064. hdl: 10871/22245 . Retrieved 28 March 2023.
  52. ↑ Kovács, E.B.; Ruhl, M.; Silva, R.L.; McElwain, J.C.; Reolid, M.; Korte, C.; Ruebsam, W.; Hesselbo, S.P. (1 March 2024). "Mercury sequestration pathways under varying depositional conditions during Early Jurassic (Pliensbachian and Toarcian) Karoo-Ferrar volcanism". Palaeogeography, Palaeoclimatology, Palaeoecology . 637: 111977. doi:10.1016/j.palaeo.2023.111977 . Retrieved 25 October 2024– via Elsevier Science Direct.
  53. ↑ 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. Bibcode:2019E&PSL.507...62T. doi: 10.1016/j.epsl.2018.11.029 . S2CID   135426425.
  54. ↑ Ruhl, Micha; Hesselbo, Stephen P.; Jenkyns, Hugh C.; Xu, Weimu; Silva, Ricardo L.; Matthews, Kara J.; Mather, Tamsin A.; Niocaill, Conall Mac; Riding, James B. (9 September 2022). "Reduced plate motion controlled timing of Early Jurassic Karoo-Ferrar large igneous province volcanism". Science Advances . 8 (36): eabo0866. Bibcode:2022SciA....8O.866R. doi:10.1126/sciadv.abo0866. hdl:10871/130801. PMC   9462690 . PMID   36083904.
  55. ↑ De Lena, Luis F.; Taylor, David; Guex, Jean; Bartolini, Annachiara; Adatte, Thierry; Van Acken, David; Spangenberg, Jorge E.; Samankassou, Elias; Vennemann, Torsten; Schaltegger, Urs (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. PMC   6895128 . PMID   31804521. S2CID   208622686.
  56. ↑ Svensen, Henrik H.; Hammer, Øyvind; Chevallier, Luc; Jerram, Dougal A.; Silkoset, Petter; Polteau, Stephane; Planke, Sverre (6 March 2020). "Understanding thermogenic degassing in large igneous provinces: Inferences from the geological and statistical characteristics of breccia pipes in the western parts of the Karoo Basin". In Adatte, Thierry; Bond, David P. G.; Keller, Gerta (eds.). Mass Extinctions, Volcanism, and Impacts: New Developments. Geological Society of America. doi:10.1130/2020.2544(03). ISBN   9780813795447. S2CID   218829332.
  57. ↑ 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. Bibcode:2005Natur.435..479M. doi:10.1038/nature03618. PMID   15917805. S2CID   4339259 . Retrieved 7 January 2023.
  58. ↑ 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. Bibcode:2007E&PSL.256..554S. doi:10.1016/j.epsl.2007.02.013 . Retrieved 20 January 2023.
  59. ↑ Gröcke, Darren R.; Rimmer, Susan M.; Yoksoulian, Lois E.; Cairncross, Bruce; Tsikos, Harilaos; Van Hunen, Jaroen (15 January 2009). "No evidence for thermogenic methane release in coal from the Karoo-Ferrar large igneous province". Earth and Planetary Science Letters . 277 (1–2): 204–212. Bibcode:2009E&PSL.277..204G. doi:10.1016/j.epsl.2008.10.022 . Retrieved 10 March 2024.
  60. ↑ 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. Bibcode:2000Natur.406..392H. doi:10.1038/35019044. PMID   10935632. S2CID   4426788 . Retrieved 7 January 2023.
  61. 1 2 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. Bibcode:2007JGSoc.164.1093C. doi:10.1144/0016-76492006-123. S2CID   129509486 . Retrieved 20 January 2023.
  62. ↑ 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. Bibcode:2020ESRv..20903283R. doi:10.1016/j.earscirev.2020.103283. S2CID   225572000 . Retrieved 23 June 2023.
  63. ↑ 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. Bibcode:2018GPC...170..163I. doi:10.1016/j.gloplacha.2018.08.012. S2CID   133856684 . Retrieved 14 June 2023.
  64. ↑ 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. Bibcode:2011PalOc..26.4210K. doi: 10.1029/2011PA002122 .
  65. ↑ 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. Bibcode:2008JGSoc.165..875M. doi:10.1144/0016-76492007-157. S2CID   131586390 . Retrieved 20 January 2023.
  66. ↑ 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. Bibcode:2005PalOc..20.3008V. doi:10.1029/2004PA001102 . Retrieved 7 January 2023.
  67. ↑ 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. Bibcode:2002AmJS..302...28B. doi:10.2475/ajs.302.1.28 . Retrieved 7 January 2023.
  68. ↑ 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. Bibcode:2005AmJS..305.1014W. doi:10.2475/ajs.305.10.1014 . Retrieved 7 January 2023.
  69. ↑ 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. Bibcode:2021NatCo..12.6221H. doi:10.1038/s41467-021-26467-6. PMC   8553747 . PMID   34711826.
  70. ↑ 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. Bibcode:2019NatSR...912518K. doi:10.1038/s41598-019-48956-x. PMC   6715628 . PMID   31467345.
  71. ↑ Ruebsam, Wolfgang; Reolid, Matías; Schwark, Lorenz (10 January 2020). "δ13C of terrestrial vegetation records Toarcian CO2 and climate gradients". Scientific Reports . 10 (1): 117. Bibcode:2020NatSR..10..117R. doi:10.1038/s41598-019-56710-6. PMC   6954244 . PMID   31924807.
  72. ↑ 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. Bibcode:2019GPC...172..440R. doi:10.1016/j.gloplacha.2018.11.003. S2CID   133660136 . Retrieved 7 January 2023.
  73. ↑ Ruebsam, Wolfgang; Münzberger, Petra; Schwark, Lorenz (23 August 2014). "Chronology of the Early Toarcian environmental crisis in the Lorraine Sub-Basin (NE Paris Basin)". Earth and Planetary Science Letters . 404: 273–282. Bibcode:2014E&PSL.404..273R. doi:10.1016/j.epsl.2014.08.005 . Retrieved 10 March 2024.
  74. ↑ Remírez, Mariano N.; Gilleaudeau, Geoffrey J.; Gan, Tian; Kipp, Michael A.; Tissot, François L. H.; Kaufman, Alan J.; Parente, Mariano (24 June 2024). "Carbonate uranium isotopes record global expansion of marine anoxia during the Toarcian Oceanic Anoxic Event". Proceedings of the National Academy of Sciences of the United States of America . 121 (27): e2406032121. doi:10.1073/pnas.2406032121. ISSN   0027-8424. PMC  11228476. PMID   38913904 . Retrieved 30 June 2024.
  75. ↑ 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 . Retrieved 4 January 2023.
  76. ↑ 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. Bibcode:2014PPP...414..332K. doi:10.1016/j.palaeo.2014.09.019. hdl: 2164/4381 . Retrieved 8 January 2023.
  77. ↑ 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. Bibcode:2005PalOc..20.2011T. doi: 10.1029/2004PA001120 .
  78. ↑ 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. Bibcode:2020PPP...55409781R. doi:10.1016/j.palaeo.2020.109781. S2CID   219059687 . Retrieved 27 September 2022.
  79. ↑ 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. Bibcode:2020IJCG..22903573R. doi:10.1016/j.coal.2020.103573. S2CID   225331537 . Retrieved 14 May 2023.
  80. ↑ Silva, Ricardo L.; Gómez, Juan J.; Fraguas, Ángela (20 November 2024). "New insights on Late Pliensbachian-Early Toarcian seawater chemistry based on belemnite rostra element content". Chemical Geology . 668: 122327. doi: 10.1016/j.chemgeo.2024.122327 .
  81. ↑ 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. Bibcode:2015E&PSL.411..164B. doi:10.1016/j.epsl.2014.11.028. ISSN   0012-821X . Retrieved 26 November 2023.
  82. ↑ Them, Theodore R.; Gill, Benjamin C.; Selby, David; Gröcke, Darren R.; Friedman, Richard M.; Owens, Jeremy D. (10 July 2017). "Evidence for rapid weathering response to climatic warming during the Toarcian Oceanic Anoxic Event". Scientific Reports . 7 (1): 5003. Bibcode:2017NatSR...7.5003T. doi:10.1038/s41598-017-05307-y. hdl: 10919/81873 . ISSN   2045-2322. PMC   5504049 . PMID   28694487.
  83. 1 2 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. Bibcode:2019NatGe..12..462S. doi:10.1038/s41561-019-0349-z. S2CID   155624907 . Retrieved 17 December 2022.
  84. ↑ Montero-Serrano, Jean-Carlos; Föllmi, Karl B.; Adatte, Thierry; Spangenberg, Jorge E.; Tribovillard, Nicolas; Fantasia, Alicia; Suan, Guillaume (16 April 2015). "Continental weathering and redox conditions during the early Toarcian Oceanic Anoxic Event in the northwestern Tethys: Insight from the Posidonia Shale section in the Swiss Jura Mountains". Palaeogeography, Palaeoclimatology, Palaeoecology . 429: 83–99. Bibcode:2015PPP...429...83M. doi:10.1016/j.palaeo.2015.03.043 . Retrieved 10 March 2024– via Elsevier Science Direct.
  85. ↑ Ruebsam, Wolfgang; Schwark, Lorenz (5 May 2024). "Disparity between Toarcian Oceanic Anoxic Event and Toarcian carbon isotope excursion". International Journal of Earth Sciences . 113 (8): 2065–2076. doi: 10.1007/s00531-024-02408-8 . ISSN   1437-3254.
  86. ↑ 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. Retrieved 14 May 2023.
  87. ↑ 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. S2CID   128946998 . Retrieved 8 April 2023.
  88. ↑ 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. Bibcode:2012PalOc..27.2211D. doi: 10.1029/2012PA002283 .
  89. ↑ 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. Bibcode:2007PPP...251..398A. doi:10.1016/j.palaeo.2007.04.014. ISSN   0031-0182 . Retrieved 26 November 2023.
  90. ↑ 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. Bibcode:2016RPaPa.235...51B. doi:10.1016/j.revpalbo.2016.09.011. ISSN   0034-6667 . Retrieved 26 November 2023.
  91. ↑ 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. Bibcode:2020ESRv..20303117R. doi:10.1016/j.earscirev.2020.103117. S2CID   214230643 . Retrieved 14 May 2023.
  92. ↑ 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. Bibcode:2022GPC...21703954R. doi:10.1016/j.gloplacha.2022.103954. S2CID   252571812 . Retrieved 5 August 2023.
  93. ↑ Li, Binbing; Jin, Xin; Corso, Jacopo Dal; Ogg, James G.; Lang, Xianguo; Baranyi, Viktória; Preto, Nereo; Franceschi, Marco; Qiao, Peijun; Shi, Zhiqiang (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. Bibcode:2023GPC...22104045L. doi:10.1016/j.gloplacha.2023.104045. ISSN   0921-8181. S2CID   256129000 . Retrieved 26 November 2023.
  94. ↑ 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". In Reolid, Matias; Duarte, Luis V.; Mattioli, Emanuela; Ruebsam, Wolfgang (eds.). Carbon Cycle and Ecosystem Response to the Jenkyns Event in the Early Toarcian (Jurassic). Geological Society of London, Special Publications. Vol. 514. The Geological Society of London. p. 335. Bibcode:2021GSLSP.514..335X. doi:10.1144/SP514-2021-2. ISBN   9781786209993. S2CID   236377708 . Retrieved 26 November 2023.
  95. ↑ 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. Bibcode:2011E&PSL.312..484G. doi:10.1016/j.epsl.2011.10.030 . Retrieved 4 January 2023.
  96. ↑ 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. Bibcode:2022GPC...21503884C. doi:10.1016/j.gloplacha.2022.103884. S2CID   250239852 . Retrieved 25 March 2023.
  97. ↑ 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". Global and Planetary Change . 170: 246–259. Bibcode:2018GPC...170..246S. doi:10.1016/j.gloplacha.2018.09.003. S2CID   134096973 . Retrieved 26 March 2023.
  98. ↑ 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). Bibcode:2022AGUA....300671T. doi:10.1029/2022AV000671. hdl: 10919/112946 . S2CID   253829543 . Retrieved 16 August 2023.
  99. ↑ 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. Bibcode:2017PalOc..32..813D. doi: 10.1002/2016PA003048 . S2CID   134242946.
  100. ↑ 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. Bibcode:2023GPC...22104026F. doi:10.1016/j.gloplacha.2022.104026. S2CID   255324488 . Retrieved 2 April 2023.
  101. ↑ 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; Slomp, Caroline P. (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. Bibcode:2018PaPa...33..994R. doi: 10.1029/2018PA003394 . S2CID   133780455.
  102. ↑ Chen, Wenhan; Kemp, David B.; He, Tianchen; Newton, Robert J.; Xiong, Yijun; Jenkyns, Hugh C.; Izumi, Kentaro; Cho, Tenichi; Huang, Chunju; Poulton, Simon W. (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. Bibcode:2023E&PSL.60217959C. doi:10.1016/j.epsl.2022.117959. S2CID   254963615. Archived from the original on 15 May 2023. Retrieved 14 May 2023.{{cite journal}}: CS1 maint: bot: original URL status unknown (link)
  103. ↑ Kunert, Alexandra; Kendall, Brian (13 February 2023). "Global ocean redox changes before and during the Toarcian Oceanic Anoxic Event". Nature Communications . 14 (1): 815. Bibcode:2023NatCo..14..815K. doi:10.1038/s41467-023-36516-x. PMC   9925726 . PMID   36781894 . Retrieved 23 June 2023.
  104. ↑ 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. Bibcode:2004JGSoc.161..685M. doi:10.1144/0016-764903-074. S2CID   128901793 . Retrieved 29 March 2023.
  105. ↑ 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". Earth and Planetary Science Letters . 357–358: 214–225. Bibcode:2012E&PSL.357..214T. doi:10.1016/j.epsl.2012.09.043.
  106. ↑ 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". Sedimentology. 68: 63–107. doi:10.1111/sed.12786. ISSN   0037-0746. S2CID   224870464.
  107. ↑ 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. Bibcode:2022SciA....8N2370P. doi: 10.1126/sciadv.abn2370 . hdl: 1874/421467 . PMC   10883373 . PMID   35776794. S2CID   250218660.
  108. ↑ 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. Bibcode:2021GPC...20703685C. doi:10.1016/j.gloplacha.2021.103685. ISSN   0921-8181. S2CID   240111632 . Retrieved 26 November 2023.
  109. 1 2 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. Bibcode:2015E&PSL.425..120K. doi:10.1016/j.epsl.2015.06.003 . Retrieved 20 January 2023.
  110. ↑ 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. Bibcode:2020ESRv..20803254K. doi:10.1016/j.earscirev.2020.103254. S2CID   225669068 . Retrieved 17 December 2022.
  111. ↑ 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. Bibcode:2019PPP...524..183D. doi:10.1016/j.palaeo.2019.03.039. hdl: 10026.1/13668 . S2CID   134835736 . Retrieved 23 November 2022.
  112. ↑ 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. Bibcode:2016PPP...457..233V. doi:10.1016/j.palaeo.2016.06.022 . Retrieved 29 October 2022.
  113. ↑ 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. Bibcode:2018PPP...506..242G. doi:10.1016/j.palaeo.2018.06.045. hdl: 10045/77781 . S2CID   135368506 . Retrieved 29 October 2022.
  114. ↑ 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. Bibcode:2019Pbio...45..296P. doi: 10.1017/pab.2019.11 . S2CID   132593370.
  115. ↑ Ullmann, C. V.; Boyle, R.; Duarte, Luís Vítor; Hesselbo, Stephen P.; Kasemann, S. A.; Klein, T.; Lenton, T. M.; Piazza, Veronica; Aberhan, Martin (16 April 2020). "Warm afterglow from the Toarcian Oceanic Anoxic Event drives the success of deep-adapted brachiopods". Scientific Reports . 10 (1): 6549. Bibcode:2020NatSR..10.6549U. doi:10.1038/s41598-020-63487-6. PMC   7162941 . PMID   32300235.
  116. ↑ 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. Bibcode:2022JIbG...48..445G. doi: 10.1007/s41513-022-00197-0 . S2CID   252072648.
  117. 1 2 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. Bibcode:2006SGC....14..399Z. doi:10.1134/S0869593806040046. S2CID   129785254 . Retrieved 14 June 2023.
  118. 1 2 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. Bibcode:2008PrGA..119...73W. doi:10.1016/S0016-7878(08)80259-3 . Retrieved 23 November 2022.
  119. ↑ 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. Bibcode:2017PPP...478..103M. doi:10.1016/j.palaeo.2017.01.009 . Retrieved 8 April 2023.
  120. ↑ 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. Bibcode:2009PPP...284...29M. doi:10.1016/j.palaeo.2009.08.023 . Retrieved 14 June 2023.
  121. ↑ 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. Bibcode:2012SolED...4.1205G. doi: 10.5194/sed-4-1205-2012 . Retrieved 26 November 2023.
  122. ↑ 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)". Journal of the Geological Society . 167 (1): 21–33. Bibcode:2010JGSoc.167...21D. doi:10.1144/0016-76492009-068. ISSN   0016-7649. S2CID   128908746.
  123. 1 2 De Baets, Kenneth; Nätscher, Paulina S.; Rita, Patricia; Fara, Emmanuel; Neige, Pascal; Bardin, Jérémie; Dera, Guillaume; Duarte, Luís Vítor; Hughes, Zoe; Laschinger, Peter; García-Ramos, José Carlos; Piñuela, Laura; Übelacker, Christof; Weis, Robert (20 December 2021). "The impact of the Pliensbachian–Toarcian crisis on belemnite assemblages and size distribution". Swiss Journal of Palaeontology . 140 (25): 1–14. Bibcode:2021SwJP..140...25D. doi: 10.1186/s13358-021-00242-y . hdl: 10316/96856 .
  124. ↑ 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. Bibcode:2021GPC...20703647V. doi: 10.1016/j.gloplacha.2021.103647 . S2CID   240513784.
  125. ↑ 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. Bibcode:2014PPP...411...79R. doi:10.1016/j.palaeo.2014.06.023. ISSN   0031-0182 . Retrieved 30 December 2023– via Elsevier Science Direct.
  126. 1 2 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. Bibcode:2019PPP...520...30R. doi:10.1016/j.palaeo.2019.01.022. S2CID   135143670 . Retrieved 17 December 2022.
  127. ↑ Goričan, Špela; Carter, Elizabeth S.; Guex, Jean; O’Dogherty, Luis; De Wever, Patrick; Dumitrica, Paulian; Hori, Rie S.; Matsuoka, Atsushi; Whalen, Patricia A. (15 September 2013). "Evolutionary patterns and palaeobiogeography of Pliensbachian and Toarcian (Early Jurassic) Radiolaria". Palaeogeography, Palaeoclimatology, Palaeoecology . 386: 620–636. Bibcode:2013PPP...386..620G. doi:10.1016/j.palaeo.2013.06.028 . Retrieved 17 December 2022.
  128. ↑ 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 . S2CID   128492520.
  129. ↑ 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. Bibcode:2019PPP...53209277R. doi:10.1016/j.palaeo.2019.109277. S2CID   200072488 . Retrieved 23 November 2022.
  130. ↑ Müller, Tamás; Karancz, Szabina; Mattioli, Emanuela; Milovský, Rastislav; Pálfy, József; Schlögl, Jan; Segit, Tomasz; Šimo, Vladimír; Tomašových, Adam (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. Bibcode:2020GPC...19503366M. doi: 10.1016/j.gloplacha.2020.103366 . S2CID   228834948.
  131. ↑ 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. Bibcode:2013PLoSO...856255D. doi: 10.1371/journal.pone.0056255 . PMC   3572952 . PMID   23457537.
  132. ↑ Atkinson, Jed W.; Little, Crispin T. S.; Dunhill, Alexander M. (3 March 2023). "Long duration of benthic ecological recovery from the early Toarcian (Early Jurassic) mass extinction event in the Cleveland Basin, UK". Journal of the Geological Society . 180 (2). Bibcode:2023JGSoc.180..126A. doi: 10.1144/jgs2022-126 . ISSN   0016-7649.
  133. ↑ Dunhill, Alexander M.; Zarzyczny, Karolina; Shaw, Jack O.; Atkinson, Jed W.; Little, Crispin T. S.; Beckerman, Andrew P. (4 October 2024). "Extinction cascades, community collapse, and recovery across a Mesozoic hyperthermal event". Nature Communications . 15 (1): 8599. doi:10.1038/s41467-024-53000-2. ISSN   2041-1723. PMC   11452722 . PMID   39366971.
  134. ↑ 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. Bibcode:1996GSLSP.102..231H. doi:10.1144/GSL.SP.1996.001.01.16. S2CID   128878485 . Retrieved 14 May 2023.
  135. ↑ 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. S2CID   131623205.
  136. ↑ Reolid, Matias; Ruebsam, Wolfgang; Benton, Michael James (22 December 2022). "Dinosaur extinctions related to the Jenkyns Event (early Toarcian, Jurassic)". Spanish Journal of Palaeontology. 37 (2): 123–140. doi: 10.7203/sjp.25683 . S2CID   255022626 . Retrieved 2 April 2023.
  137. ↑ 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". Proceedings of the Royal Society B: Biological Sciences . 287 (1939): 20202310. doi:10.1098/rspb.2020.2310. ISSN   0962-8452. PMC   7739499 . PMID   33203331.
  138. ↑ Wignall, Paul B. (29 September 2015). "Pangea's Final Blow". The Worst of Times: How Life on Earth Survived Eighty Million Years of Mass Extinctions. Princeton: Princeton University Press. pp. 137–153. ISBN   978-0691142098.
  139. ↑ Swaby, Emily J.; Coe, Angela L.; Ansorge, Jörg; Caswell, Bryony A.; Hayward, Scott A. L.; Mander, Luke; Stevens, Liadan G.; McArdle, Aimee (17 April 2024). Thuy, Ben (ed.). "The fossil insect assemblage associated with the Toarcian (Lower Jurassic) oceanic anoxic event from Alderton Hill, Gloucestershire, UK". PLOS ONE . 19 (4): e0299551. Bibcode:2024PLoSO..1999551S. doi: 10.1371/journal.pone.0299551 . ISSN   1932-6203. PMC   11023202 . PMID   38630753.
  140. ↑ Jin, Xin; Zhang, Fei; Baranyi, Viktória; Kemp, David B.; Feng, Xinbin; Grasby, Stephen E.; Sun, Guangyi; Shi, Zhiqiang; Chen, Wenhan; Dal Corso, Jacopo (15 November 2022). "Early Jurassic massive release of terrestrial mercury linked to floral crisis". Earth and Planetary Science Letters . 598: 117842. Bibcode:2022E&PSL.59817842J. doi:10.1016/j.epsl.2022.117842. S2CID   252794071 . Retrieved 14 June 2023.
  141. ↑ 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. Bibcode:2023Geo....51..652B. doi:10.1130/G51037.1. S2CID   258580509 . Retrieved 14 June 2023.
  142. ↑ 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. Bibcode:2021NatSR..1124087S. doi:10.1038/s41598-021-03482-7. PMC   8677819 . PMID   34916533 . Retrieved 17 July 2023.
  143. ↑ 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. Bibcode:2013ChGeo.341....1L. doi:10.1016/j.chemgeo.2013.01.003 . Retrieved 17 December 2022.
  144. ↑ 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. Bibcode:2021SedG..41905909F. doi:10.1016/j.sedgeo.2021.105909. S2CID   234855326 . Retrieved 2 April 2023.
  145. ↑ 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. Bibcode:2001AmJS..301..112J. doi:10.2475/ajs.301.2.112. S2CID   123838 . Retrieved 8 April 2023.
  146. ↑ 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. Bibcode:2021MarPG.13305304Y. doi:10.1016/j.marpetgeo.2021.105304 . Retrieved 8 January 2023.
  147. ↑ 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. Bibcode:2022JAESc.23205035Q. doi:10.1016/j.jseaes.2021.105035. S2CID   245038615 . Retrieved 5 August 2023.
  148. ↑ Xu, Weimu; Ruhl, Micha; Jenkyns, Hugh C.; Leng, Melanie J.; Huggett, Jennifer M.; Minisini, Daniel; Ullmann, Clemens V.; Riding, James B.; Weijers, Johan W. H.; Storm, Marisa S.; Percival, Lawrence M. E.; Tosca, Nicholas J.; Idiz, Erdem F.; Tegelaar, Erik W.; Hesselbo, Stephen P. (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. Bibcode:2018E&PSL.484..396X. doi: 10.1016/j.epsl.2017.12.037 . hdl: 10871/30888 . ISSN   0012-821X. S2CID   55022954.
  149. ↑ 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. Bibcode:2019ESRv..19802932F. doi:10.1016/j.earscirev.2019.102932. S2CID   202179439 . Retrieved 29 March 2023.
  150. ↑ 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. Bibcode:2009PPP...271...39D. doi:10.1016/j.palaeo.2008.09.010 . Retrieved 17 July 2023.
  151. ↑ Müller, Tamás; Price, Gregory D.; Bajnai, Dávid; Nyerges, Anita; Kesjár, Dóra; Raucsik, Béla; Varga, Andrea; Judik, Katalin; Fekete, József; May, Zoltán; Pálfy, József (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. hdl: 10026.1/8649 . S2CID   133481660 . Retrieved 8 April 2023.
  152. ↑ 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. Bibcode:2018JGSoc.175..883F. doi:10.1144/jgs2018-008. S2CID   134669817 . Retrieved 29 March 2023.
  153. ↑ 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. Bibcode:2008PalOc..23.3208M. doi: 10.1029/2007PA001435 .
  154. ↑ 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. Bibcode:2022GPC...21503860L. doi:10.1016/j.gloplacha.2022.103860. S2CID   249558555. Archived from the original on 18 December 2022. Retrieved 17 December 2022.{{cite journal}}: CS1 maint: bot: original URL status unknown (link)
  155. ↑ 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. Bibcode:2021GSLSP.514..335X. doi:10.1144/SP514-2021-2. S2CID   236377708 . Retrieved 2 April 2023.
  156. 1 2 Xu, Weimu; Ruhl, Micha; Jenkyns, Hugh C.; Hesselbo, Stephen P.; Riding, James B.; Selby, David; Naafs, B. David A.; Weijers, Johan W. H.; Pancost, Richard D.; Tegelaar, Erik W.; Idiz, Erdem F. (February 2017). "Carbon sequestration in an expanded lake system during the Toarcian oceanic anoxic event". Nature Geoscience . 10 (2): 129–134. Bibcode:2017NatGe..10..129X. doi:10.1038/ngeo2871. hdl: 10871/24965 . ISSN   1752-0894.
  157. ↑ 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. Bibcode:2022GPC...21603915L. doi:10.1016/j.gloplacha.2022.103915. S2CID   251560158 . Retrieved 16 August 2023.
This page is based on this Wikipedia article
Text is available under the CC BY-SA 4.0 license; additional terms may apply.
Images, videos and audio are available under their respective licenses.