Editing Triassic (section)

==Climate==
The Triassic continental interior climate was generally hot and dry, so that typical deposits are [[red beds|red bed]] [[sandstone]]s and [[evaporite]]s. There is no evidence of [[glacier|glaciation]] at or near either pole; in fact, the polar regions were apparently moist and [[temperate]], providing a climate suitable for forests and vertebrates, including reptiles. Pangaea's large size limited the moderating effect of the global ocean; its [[continental climate]] was highly seasonal, with very hot summers and cold winters.<ref name="Stanley, 452-3">Stanley, 452–53.</ref> The strong contrast between the Pangea supercontinent and the global ocean triggered intense cross-equatorial [[monsoons]],<ref name="Stanley, 452-3"/> sometimes referred to as the [[Pangean megamonsoon]]s.<ref>{{cite journal |last1=Zeng |first1=Zhiwei |last2=Zhu |first2=Hongtao |last3=Yang |first3=Xianghua |last4=Zeng |first4=Hongliu |last5=Hu |first5=Xiaolin |last6=Xia |first6=Chenchen |date=May 2019 |title=The Pangaea Megamonsoon records: Evidence from the Triassic Mungaroo Formation, Northwest Shelf of Australia |url=https://www.sciencedirect.com/science/article/abs/pii/S1342937X19300127 |journal=[[Gondwana Research]] |volume=69 |pages=1–24 |doi=10.1016/j.gr.2018.11.015 |bibcode=2019GondR..69....1Z |s2cid=134145664 |access-date=9 January 2023}}</ref>

The Triassic may have mostly been a dry period, but evidence exists that it was punctuated by several episodes of increased rainfall in tropical and subtropical latitudes of the Tethys Sea and its surrounding land.<ref name=Pretoetal2010>{{cite journal |last1=Preto |first1=N. |last2=Kustatscher |first2=E. |last3=Wignall |first3=P. B. |year=2010 |title=Triassic climates – State of the art and perspectives |journal=Palaeogeography, Palaeoclimatology, Palaeoecology |volume=290 |issue=1–4 |pages=1–10 |doi=10.1016/j.palaeo.2010.03.015 |bibcode=2010PPP...290....1P}}</ref> Sediments and fossils suggestive of a more humid climate are known from the Anisian to Ladinian of the Tethysian domain, and from the Carnian and Rhaetian of a larger area that includes also the Boreal domain (e.g., [[Svalbard]] Islands), the [[North America]]n continent, the South [[China]] block and [[Argentina]]. The best-studied of such episodes of humid climate, and probably the most intense and widespread, was the [[Carnian Pluvial Event]]. 

=== Early Triassic ===
The Early Triassic was the hottest portion of the entire Phanerozoic, seeing as it occurred during and immediately after the discharge of titanic volumes of greenhouse gases from the Siberian Traps. The Early Triassic began with the Permian-Triassic Thermal Maximum (PTTM) and was followed by the brief Dienerian Cooling (DC) from 251 to 249 Ma, which was in turn followed by the Latest Smithian Thermal Maximum (LSTT) around 249 to 248 Ma. During the Latest Olenekian Cooling (LOC), from 248 to 247 Ma, temperatures cooled by about 6 °C.<ref name="ChristopherRobertScotese">{{Cite journal |last1=Scotese |first1=Christopher Robert |last2=Song |first2=Haijun |last3=Mills |first3=Benjamin J. W. |last4=van der Meer |first4=Douwe G. |date=1 April 2021 |title=Phanerozoic paleotemperatures: The earth's changing climate during the last 540 million years |url=https://www.sciencedirect.com/science/article/pii/S0012825221000027 |journal=[[Earth-Science Reviews]] |volume=215 |pages=103503 |doi=10.1016/j.earscirev.2021.103503 |bibcode=2021ESRv..21503503S |s2cid=233579194 |issn=0012-8252 |access-date=22 September 2023}}</ref>

=== Middle Triassic ===
The Middle Triassic was cooler than the Early Triassic, with temperatures falling over most of the Anisian, with the exception of a warming spike in the latter portion of the stage.<ref>{{Cite journal |last1=Trotter |first1=Julie A. |last2=Williams |first2=Ian S. |last3=Nicora |first3=Alda |last4=Mazza |first4=Michele |last5=Rigo |first5=Manuel |date=April 2015 |title=Long-term cycles of Triassic climate change: a new δ18O record from conodont apatite |url=https://linkinghub.elsevier.com/retrieve/pii/S0012821X15000667 |journal=[[Earth and Planetary Science Letters]] |language=en |volume=415 |pages=165–174 |doi=10.1016/j.epsl.2015.01.038 |bibcode=2015E&PSL.415..165T |access-date=22 September 2023}}</ref> From 242 to 233 Ma, the Ladinian-Carnian Cooling (LCC) ensued.<ref name="ChristopherRobertScotese" /> 

=== Late Triassic ===
At the beginning of the Carnian, global temperatures continued to be relatively cool.<ref>{{Cite journal |last1=Dal Corso |first1=Jacopo |last2=Mills |first2=Benjamin J.W. |last3=Chu |first3=Daoliang |last4=Newton |first4=Robert J. |last5=Song |first5=Haijun |date=15 January 2022 |title=Background Earth system state amplified Carnian (Late Triassic) environmental changes |url=https://linkinghub.elsevier.com/retrieve/pii/S0012821X2100577X |journal=[[Earth and Planetary Science Letters]] |language=en |volume=578 |pages=117321 |doi=10.1016/j.epsl.2021.117321 |bibcode=2022E&PSL.57817321D |s2cid=244847207 |access-date=22 September 2023}}</ref> The eruption of the Wrangellia Large Igneous Province around 234 Ma caused abrupt global warming, terminating the cooling trend of the LCC.<ref>{{Cite journal |last1=Dal Corso |first1=J. |last2=Mietto |first2=P. |last3=Newton |first3=R. J. |last4=Pancost |first4=R. D. |last5=Preto |first5=N. |last6=Roghi |first6=G. |last7=Wignall |first7=P. B. |date=1 January 2012 |title=Discovery of a major negative 13C spike in the Carnian (Late Triassic) linked to the eruption of Wrangellia flood basalts |url=https://pubs.geoscienceworld.org/geology/article/40/1/79-82/130736 |journal=[[Geology (journal)|Geology]] |language=en |volume=40 |issue=1 |pages=79–82 |doi=10.1130/G32473.1 |bibcode=2012Geo....40...79D |issn=0091-7613 |access-date=22 September 2023}}</ref> This warming was responsible for the Carnian Pluvial Event and resulted in an episode of widespread global humidity.<ref>{{Cite journal |last1=Li |first1=Liqin |last2=Kürschner |first2=Wolfram M. |last3=Lu |first3=Ning |last4=Chen |first4=Hongyu |last5=An |first5=Pengcheng |last6=Wang |first6=Yongdong |date=September 2022 |title=Palynological record of the Carnian Pluvial Episode from the northwestern Sichuan Basin, SW China |url=https://linkinghub.elsevier.com/retrieve/pii/S0034666722001026 |journal=[[Review of Palaeobotany and Palynology]] |language=en |volume=304 |pages=104704 |doi=10.1016/j.revpalbo.2022.104704 |bibcode=2022RPaPa.30404704L |s2cid=249528886 |access-date=22 September 2023|hdl=10852/99190 |hdl-access=free }}</ref> The CPE ushered in the Mid-Carnian Warm Interval (MCWI), which lasted from 234 to 227 Ma.<ref name="ChristopherRobertScotese" /> At the Carnian-Norian boundary occurred a positive [[Δ13C|δ<sup>13</sup>C]] excursion believed to signify an increase in organic carbon burial.<ref>{{Cite journal |last1=Muttoni |first1=Giovanni |last2=Mazza |first2=Michele |last3=Mosher |first3=David |last4=Katz |first4=Miriam E. |last5=Kent |first5=Dennis V. |last6=Balini |first6=Marco |date=1 April 2014 |title=A Middle–Late Triassic (Ladinian–Rhaetian) carbon and oxygen isotope record from the Tethyan Ocean |url=https://www.sciencedirect.com/science/article/pii/S0031018214000285 |journal=[[Palaeogeography, Palaeoclimatology, Palaeoecology]] |volume=399 |pages=246–259 |doi=10.1016/j.palaeo.2014.01.018 |bibcode=2014PPP...399..246M |issn=0031-0182 |access-date=24 November 2023}}</ref> From 227 to 217 Ma, there was a relatively cool period known as the Early Norian Cool Interval (ENCI), after which occurred the Mid-Norian Warm Interval (MNWI) from 217 to 209 Ma. The MNWI was briefly interrupted around 214 Ma by a cooling possibly related to the [[Manicouagan Impact Crater|Manicouagan impact]].<ref name="ChristopherRobertScotese" /> Around 212 Ma, a 10 Myr eccentricity maximum caused a paludification of Pangaea and a reduction in the size of arid climatic zones.<ref>{{Cite journal |last1=Ikeda |first1=Masayuki |last2=Ozaki |first2=Kazumi |last3=Legrand |first3=Julien |date=23 July 2020 |title=Impact of 10-Myr scale monsoon dynamics on Mesozoic climate and ecosystems |journal=[[Scientific Reports]] |language=en |volume=10 |issue=1 |pages=11984 |doi=10.1038/s41598-020-68542-w |pmid=32704030 |pmc=7378230 |bibcode=2020NatSR..1011984I |issn=2045-2322 }}</ref> The Rhaetian Cool Interval (RCI) lasted from 209 to 201 Ma.<ref name="ChristopherRobertScotese" /> At the terminus of the Triassic, there was an extreme warming event referred to as the End-Triassic Thermal Event (ETTE), which was responsible for the Triassic-Jurassic mass extinction.<ref name="ChristopherRobertScotese" /> Bubbles of [[carbon dioxide]] in basaltic rocks dating back to the end of the Triassic indicate that volcanic activity from the Central Atlantic Magmatic Province helped trigger climate change in the ETTE.<ref>{{Cite journal |last1=Capriolo |first1=Manfredo |last2=Marzoli |first2=Andrea |last3=Aradi |first3=László E. |last4=Callegaro |first4=Sara |last5=Dal Corso |first5=Jacopo |last6=Newton |first6=Robert J. |last7=Mills |first7=Benjamin J. W. |last8=Wignall |first8=Paul B. |last9=Bartoli |first9=Omar |last10=Baker |first10=Don R. |last11=Youbi |first11=Nasrrddine |last12=Remusat |first12=Laurent |last13=Spiess |first13=Richard |last14=Szabó |first14=Csaba |date=7 April 2020 |title=Deep CO2 in the end-Triassic Central Atlantic Magmatic Province |journal=[[Nature Communications]] |language=en |volume=11 |issue=1 |page=1670 |doi=10.1038/s41467-020-15325-6 |issn=2041-1723 |pmc=7138847 |pmid=32265448 |bibcode=2020NatCo..11.1670C }}</ref>