Editing Triassic (section)

=== 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|url-access=subscription }}</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|url-access=subscription }}</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>