Editing Holocene (section)

=== East Asia ===
Southwestern China experienced long-term warming during the Early Holocene up until ~7,000 BP.<ref>{{Cite journal |last1=Sun |first1=Weiwei |last2=Zhang |first2=Enlou |last3=Jiang |first3=Qingfeng |last4=Ning |first4=Dongliang |last5=Luo |first5=Wenlei |date=October 2023 |title=Temperature changes during the last deglaciation and early Holocene in southwest China |url=https://linkinghub.elsevier.com/retrieve/pii/S0921818123002114 |journal=[[Global and Planetary Change]] |language=en |volume=229 |pages=104238 |doi=10.1016/j.gloplacha.2023.104238 |bibcode=2023GPC...22904238S |access-date=9 June 2024 |via=Elsevier Science Direct}}</ref> Northern China experienced an abrupt aridification event approximately 4,000 BP.<ref>{{Cite journal |last1=Guo |first1=Zhengtang |last2=Petit-Maire |first2=Nicole |last3=Kröpelin |first3=Stefan |date=November 2000 |title=Holocene non-orbital climatic events in present-day arid areas of northern Africa and China |url=https://linkinghub.elsevier.com/retrieve/pii/S0921818100000370 |journal=[[Global and Planetary Change]] |volume=26 |issue=1–3 |pages=97–103 |doi=10.1016/S0921-8181(00)00037-0 |bibcode=2000GPC....26...97G |access-date=10 September 2023}}</ref> From around 3,500 to 3,000 BP, northeastern China underwent a prolonged cooling, manifesting itself with the disruption of Bronze Age civilisations in the region.<ref>{{Cite journal |last1=Zheng |first1=Yanhong |last2=Yu |first2=Shi-Yong |last3=Fan |first3=Tongyu |last4=Oppenheimer |first4=Clive |last5=Yu |first5=Xuefeng |last6=Liu |first6=Zhao |last7=Xian |first7=Feng |last8=Liu |first8=Zhen |last9=Li |first9=Jianyong |last10=Li |first10=Jiahao |date=15 July 2021 |title=Prolonged cooling interrupted the Bronze Age cultures in northeastern China 3500 years ago |url=https://www.sciencedirect.com/science/article/pii/S0031018221002467 |journal=[[Palaeogeography, Palaeoclimatology, Palaeoecology]] |volume=574 |pages=110461 |doi=10.1016/j.palaeo.2021.110461 |bibcode=2021PPP...57410461Z |s2cid=236229299 |issn=0031-0182 |access-date=15 October 2023}}</ref> Eastern and southern China, the monsoonal regions of China, were wetter than present in the Early and Middle Holocene.<ref name="VegetationResponseMonsoonChina">{{Cite journal |last1=Zhao |first1=Yan |last2=Yu |first2=Zicheng |last3=Chen |first3=Fahu |last4=Zhang |first4=Jiawu |last5=Yang |first5=Bao |date=1 December 2009 |title=Vegetation response to Holocene climate change in monsoon-influenced region of China |url=https://www.sciencedirect.com/science/article/pii/S0012825209001627 |journal=[[Earth-Science Reviews]] |volume=97 |issue=1 |pages=242–256 |doi=10.1016/j.earscirev.2009.10.007 |bibcode=2009ESRv...97..242Z |issn=0012-8252 |access-date=10 September 2023}}</ref> Lake Huguangyan's TOC, δ<sup>13</sup>C<sub>wax</sub>, δ<sup>13</sup>C<sub>org</sub>, δ<sup>15</sup>N values suggest the period of peak moisture lasted from 9,200 to 1,800 BP and was attributable to a strong East Asian Summer Monsoon (EASM).<ref>{{Cite journal |last1=Jia |first1=Guodong |last2=Bai |first2=Yang |last3=Yang |first3=Xiaoqiang |last4=Xie |first4=Luhua |last5=Wei |first5=Gangjian |last6=Ouyang |first6=Tingping |last7=Chu |first7=Guoqiang |last8=Liu |first8=Zhonghui |last9=Peng |first9=Ping'an |date=1 March 2015 |title=Biogeochemical evidence of Holocene East Asian summer and winter monsoon variability from a tropical maar lake in southern China |url=https://www.sciencedirect.com/science/article/pii/S0277379115000098 |journal=[[Quaternary Science Reviews]] |volume=111 |pages=51–61 |doi=10.1016/j.quascirev.2015.01.002 |issn=0277-3791 |access-date=10 September 2023}}</ref> Late Holocene cooling events in the region were dominantly influenced by solar forcing, with many individual cold snaps linked to solar minima such as the Oort, [[Wolf minimum|Wolf]], [[Spörer Minimum|Spörer]], and [[Maunder Minimum|Maunder Minima]].<ref>{{Cite journal |last=Park |first=Jungjae |date=1 March 2017 |title=Solar and tropical ocean forcing of late-Holocene climate change in coastal East Asia |url=https://www.sciencedirect.com/science/article/pii/S0031018217300044 |journal=[[Palaeogeography, Palaeoclimatology, Palaeoecology]] |volume=469 |pages=74–83 |doi=10.1016/j.palaeo.2017.01.005 |bibcode=2017PPP...469...74P |issn=0031-0182 |access-date=15 September 2023}}</ref> A notable cooling event in southeastern China occurred 3,200 BP.<ref>{{Cite journal |last1=Wang |first1=Mengyuan |last2=Zheng |first2=Zhuo |last3=Man |first3=Meiling |last4=Hu |first4=Jianfang |last5=Gao |first5=Quanzhou |date=5 July 2017 |title=Branched GDGT-based paleotemperature reconstruction of the last 30,000 years in humid monsoon region of Southeast China |url=https://linkinghub.elsevier.com/retrieve/pii/S0009254117303017 |journal=[[Chemical Geology]] |language=en |volume=463 |pages=94–102 |doi=10.1016/j.chemgeo.2017.05.014 |bibcode=2017ChGeo.463...94W |access-date=19 July 2024 |via=Elsevier Science Direct}}</ref> Strengthening of the winter monsoon occurred around 5,500, 4,000, and 2,500 BP.<ref>{{Cite journal |last1=Li |first1=Zhen |last2=Pospelova |first2=Vera |last3=Liu |first3=Lejun |last4=Zhou |first4=Rui |last5=Song |first5=Bing |date=1 October 2017 |title=High-resolution palynological record of Holocene climatic and oceanographic changes in the northern South China Sea |url=https://linkinghub.elsevier.com/retrieve/pii/S0031018217302626 |journal=[[Palaeogeography, Palaeoclimatology, Palaeoecology]] |language=en |volume=483 |pages=94–124 |doi=10.1016/j.palaeo.2017.03.009 |bibcode=2017PPP...483...94L |access-date=19 July 2024 |via=Elsevier Science Direct}}</ref> Monsoonal regions of China became more arid in the Late Holocene.<ref name="VegetationResponseMonsoonChina" />

In the Sea of Japan, the Middle Holocene was notable for its warmth, with rhythmic temperature fluctuations every 400–500 and 1,000 years.<ref>{{Cite journal |last=Koizumi |first=Itaru |date=December 2008 |title=Diatom-derived SSTs (Td′ ratio) indicate warm seas off Japan during the middle Holocene (8.2–3.3 kyr BP) |url=https://www.sciencedirect.com/science/article/pii/S037783980800100X |journal=Marine Micropaleontology |language=en |volume=69 |issue=3–4 |pages=263–281 |doi=10.1016/j.marmicro.2008.08.004 |bibcode=2008MarMP..69..263K |access-date=11 October 2024 |via=Elsevier Science Direct}}</ref>