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Global distribution of the 4.2 kiloyear event. The hatched areas were affected by wet conditions or flooding, and the dotted areas by drought or dust storms.[1]

The 4.2-kiloyear (thousand years) BP aridification event (long-term drought), also known as the 4.2 ka event,[2] was one of the most severe climatic events of the Holocene epoch.[3] It defines the beginning of the current Meghalayan age in the Holocene epoch.

Starting around 2200 BC, it most likely lasted the entire 22nd century BC. It has been hypothesised to have caused the collapse of the Old Kingdom in Egypt, the Akkadian Empire in Mesopotamia, and the Liangzhu culture in the lower Yangtze River area.[4][5] The drought may also have initiated the collapse of the Indus Valley Civilisation, with some of its population moving southeastward to follow the movement of their desired habitat,[6] as well as the migration of Indo-European-speaking people into India.[7] Some scientists disagree with that conclusion, citing evidence that the event was not a global drought and did not happen in a clear timeline.[8]

Causes

Modelling evidence suggests that the 4.2 ka event was the result of a significant weakening of the Atlantic meridional overturning circulation (AMOC), disrupting global ocean currents and generating precipitation and temperature changes in various regions.[9][10] The Intertropical Convergence Zone (ITCZ) abruptly shifted southward.[11][12] Evidence suggests increased El Niño–Southern Oscillation (ENSO) variability also played a role in generating the climatic conditions associated with the event.[13] Explosive volcanism in Iceland has also been proposed as a cause,[14] though the low sulphur content of Icelandic volcanoes has led other studies to suggest it had a negligible impact on global climate.[15]

Evidence

Central Greenland reconstructed temperature. Unlike the 8.2-kiloyear event, the 4.2-kiloyear event has no prominent signal in the Gisp2 ice core that has an onset at 4.2 ka BP.[citation needed]

A phase of intense aridity about 4.2 ka BP is recorded across North Africa,[16] the Middle East,[17] the Red Sea,[18] the Arabian Peninsula,[19] the Indian subcontinent,[6] and midcontinental North America.[20] Glaciers throughout the mountain ranges of western Canada advanced about that time.[21] Iceland also experienced glacial advance.[15] Evidence has also been found in an Italian cave flowstone,[22] the Kilimanjaro ice sheet,[23] and in Andean glacier ice.[24] The onset of the aridification in Mesopotamia in about 4100 BP also coincided with a cooling event in the North Atlantic, known as Bond event 3.[3][25][26] Despite the geographic diversity of these examples, evidence for the 4.2 ka event in Northern Europe is ambiguous, which suggests that the origins and effects of the event are spatially complex.[2]

In 2018, the International Commission on Stratigraphy divided the Holocene epoch into three periods,[27] with the late Holocene from approximately 2250 BC onwards designated as the Meghalayan stage/age.[28] The boundary stratotype is a speleothem in Mawmluh cave in India,[29] and the global auxiliary stratotype is an ice core from Mount Logan in Canada.[30] However, justification for this division is debated as the event was not a global drought and did not happen within a clear timeframe. Jessica Tierney, a paleoclimatologist at the University of Arizona in Tucson, states that proponents of the new partitioning mistakenly "lumped together evidence of other droughts and wet periods, sometimes centuries away from the event."[8]

Effects

Europe

British Isles

In Ireland, there is little definitive record of the 4.2 ka event outside of a brief isotopic excursion in some cave speleothem records. The manner in which this climatic event manifested itself in the region is thus unclear.[31] In Great Britain as in Ireland, the nature of the 4.2 ka event is ambiguous and unclear.[2] The yew tree's abundance declined in eastern England.[32]

Eastern Europe

Analysis of sediments from Lake Spore reveals that in Poland, winters became colder between 4250 and 4000 BP, with this cooling likely responsible for a podzolisation (generation of boreal forest soil type) event around 4200 BP, whereas summer temperatures remained constant. Humidity levels were not affected by the 4.2 ka event.[33]

Iberian Peninsula

In the Alboran Sea, the western Mediterranean, a dry phase occurred from about 4400 BP to 4300 BP but was abruptly followed by a shift towards wetter conditions, suggesting a more complex pattern of climate change than other regions during the 4.2 ka event.[34]

On the Iberian Peninsula, the construction of motillas-type settlements in the period after 2200 BC is believed to be the consequence of the severe aridification that affected this area. According to M. Mejías Moreno, who reported the first palaeohydrogeological interdisciplinary research in La Mancha, Spain, these motillas may represent the oldest, most ancient system of groundwater collection in the Iberian Peninsula and their construction might have been directly connected to the prolonged, harsh drought and other climatic perturbations brought by the 4.2 ka event. The authors' analysis verified a relationship between the geological substrate and the spatial distribution of the motillas.[35]

Italian Peninsula

In the Gulf of Genoa, mean annual temperature dropped, winters became drier, and summers became wetter and cooler, a phenomenon most likely caused by the southward retreat of the ITCZ in summer that weakened the high pressure and reduced ocean warming over the western Mediterranean, which led to retarded evaporation rates in the autumn and early winter.[36] The 4.2 ka event appears to have wettened the climate in the Alps.[37] Lake Petit saw increased precipitation during the ice-free season, evidenced by an increase in δ18Odiatom.[38] Southern Italy, in contrast, experienced intense aridification.[37] A major decline in forests occurred in Italy as a result of the climatic perturbation.[39]

North Africa

At the site of Sidi Ali in the Middle Atlas, δ18O values indicate not a dry spell but a centennial-scale period of cooler and more humid climate.[40] In c. 2150 BC, Egypt was hit by a series of exceptionally low Nile floods that may have influenced the collapse of the centralised government of the Old Kingdom after a famine.[41]

Middle East

The south-central Levant experienced two phases of dry climate punctuated by a wet interval in between and thus the 4.2 ka event in the region has been termed a W-shaped event.[42]

Enhanced dust flux coeval with δ18O peaks is recorded in Mesopotamia from 4260 to 3970 BP, reflecting intense aridity.[43] The aridification of Mesopotamia may have been related to the onset of cooler sea-surface temperatures in the North Atlantic (Bond event 3), as analysis of the modern instrumental record shows that large (50%) interannual reductions in Mesopotamian water supply result when subpolar northwest Atlantic sea surface temperatures are anomalously cool.[44] The headwaters of the Tigris and Euphrates rivers are fed by elevation-induced capture of winter Mediterranean rainfall.

The Akkadian Empire in 2300 BC was the second civilization to subsume independent societies into a single state (the first being ancient Egypt in around 3100 BC). It has been claimed that the collapse of the state was influenced by a wide-ranging, centuries-long drought.[45][46] Archaeological evidence documents widespread abandonment of the agricultural plains of northern Mesopotamia and dramatic influxes of refugees into southern Mesopotamia, around 2170 BC,[47] which may have weakened the Akkadian state.[48] A 180-km-long wall, the "Repeller of the Amorites", was built across central Mesopotamia to stem nomadic incursions to the south. Around 2150 BC, the Gutian people, who originally inhabited the Zagros Mountains, defeated the demoralised Akkadian army, took Akkad and destroyed it around 2115 BC. Widespread agricultural change in the Near East is visible at the end of the 3rd millennium BC.[49] Weiss suggests a figure of 300,000 displaced from the zone of uncertainty,[47] while Burke suggests no less than 126,400 (99,000 displaced from Upper Mesopotamia; 17,400 from Middle Euphrates and approximately 10,000 from territories from northeast to southeast of Ebla).[50] Resettlement of the northern plains by smaller sedentary populations occurred near 1900 BC, three centuries after the collapse.[47]

In the Persian Gulf region, there was a sudden change in settlement pattern, style of pottery and tombs. The 22nd century BC drought marks the end of the Umm Al Nar culture and the change to the Wadi Suq culture.[19] A study of fossil corals in Oman provides evidence that prolonged winter shamal seasons, around 4200 years ago, led to the salinization of the irrigated field, which made a dramatic decrease in crop production trigger a widespread famine and eventually the collapse of the ancient Akkadian Empire.[51][52]

South and Central Asia

The Siberian High increased in area and magnitude, which blocked moisture-carrying westerly winds, causing intense aridity in Central Asia.[53]

The Indian Summer Monsoon (ISM) and Indian Winter Monsoon (IWM) both declined in strength, leading to highly arid conditions in northwestern South Asia.[54] The ISM's decline is evident from low Mn/Ti and Mn/Fe values in Rara Lake from this time.[55] The area around PankangTeng Tso Lake in the Tawang district of Arunachal Pradesh had cold and dry conditions and was dominated by subalpine vegetation.[56] Though some proxy records suggest a prolonged, multicentennial dry period, others indicate that the 4.2 ka event was a series of multidecadal droughts instead.[57][58]

Effects on the Indus Valley civilisation

Main articles: Indus Valley Civilisation and Indo-Aryan migrations

In the 2nd millennium BC, widespread aridification occurred in the Eurasian steppes and in South Asia.[7][59] On the steppes, the vegetation changed, driving "higher mobility and transition to the nomadic cattle breeding."[59][note 1] Water shortage also strongly affected South Asia:

This time was one of great upheaval for ecological reasons. Prolonged failure of rains caused acute water shortage in large areas, causing the collapse of sedentary urban cultures in south central Asia, Afghanistan, Iran, and India, and triggering large-scale migrations. Inevitably, the new arrivals came to merge with and dominate the post-urban cultures.[7]

Urban centers of the Indus Valley Civilisation were abandoned and replaced by disparate local cultures because of the same climate change that affected the neighbouring regions to the west.[60] As of 2016, many scholars believed that drought and a decline in trade with Egypt and Mesopotamia caused the collapse of the Indus civilisation.[61] The Ghaggar-Hakra system was rain-fed,[62][63][64] and water supply depended on the monsoons. The Indus Valley climate grew significantly cooler and drier from about 1800 BC, which is linked to a contemporary general weakening of the monsoon.[62] Aridity increased, with the Ghaggar-Hakra River retracting its reach towards the foothills of the Himalayas,[62][65][66] leading to erratic and less-extensive floods, which made inundation agriculture less sustainable. Aridification reduced the water supply enough to cause the civilisation's demise, and to scatter its population eastward.[6][67][68][69]

East Asia

The 4.2 ka event resulted in an enormous reduction in the strength of the East Asian Summer Monsoon (EASM).[70] This profound weakening of the EASM has been postulated to have resulted from a reduction in the strength of the AMOC;[71] the cooling of North Atlantic waters led to retardation of northward movements of the EASM and diminished rainfall on its northern margin.[70] A stark humidity gradient emerged between northern and southern China because of the EASM's southward move.[72] Northeastern China was strongly affected;[73] proxy records from Hulun Lake in Inner Mongolia reveal a major dry event from 4210–3840 BP.[70] δ18O values from Yonglu Cave in Hubei confirm that the region became characterised by increased aridity and show that the onset of the event was gradual but that its end was sudden.[74]

In the Korean Peninsula, the 4.2 ka event was associated with significant aridification, measured by the large decline in arboreal pollen percentage (AP).[75]

The Sannai-Maruyama site in Japan declined during the same period;[76] the growing population of the Jomon culture gradually turned to decline after that.[77]

Rebun Island experienced an abrupt, intense cooling around 4,130 BP believed to be associated with the 4.2 ka event.[78]

Effects on Chinese civilisation

The drought may have caused the collapse of Neolithic cultures around Central China in the late 3rd millennium BC.[79][80] In the Yishu River Basin (a river basin that consists of the Yi River (沂河) of Shandong and Shu River), the flourishing Longshan culture was affected by a cooling that severely reduced rice output and led to a substantial decrease in population and to fewer archaeological sites.[81] In about 2000 BC, Longshan was displaced by the Yueshi culture, which had fewer and less-sophisticated artifacts of ceramic and bronze.The Liangzhu civilization in the lower reaches of the Yangtze River also declined during the same period.[82] The 4.2 ka event is also believed to have helped collapse the Dawenkou culture.[83] The 4.2 ka event had no discernible impact on the spread of millet cultivation in the region.[84]

Southern Africa

Stalagmites from northeastern Namibia demonstrate the region became wetter thanks to the southward shift of the ITCZ.[85] The Namibian humidification event had two pulses.[86]

Mascarenes

No signal of the 4.2 ka event has been found in Rodrigues.[87]

See also

Explanatory notes

  1. ^ Demkina et al. (2017): "In the second millennium BC, humidization of the climate led to the divergence of the soil cover with secondary formation of the complexes of chestnut soils and solonetzes. This paleoecological crisis had a significant effect on the economy of the tribes in the Late Catacomb and Post-Catacomb time stipulating their higher mobility and transition to the nomadic cattle breeding."[59]

References

  1. ^ Another map for reference in Railsback, L. Bruce; Liang, Fuyuan; Brook, G. A.; Voarintsoa, Ny Riavo G.; Sletten, Hillary R.; Marais, Eugene; Hardt, Ben; Cheng, Hai; Edwards, R. Lawrence (15 April 2018). "The timing, two-pulsed nature, and variable climatic expression of the 4.2 ka event: A review and new high-resolution stalagmite data from Namibia". Quaternary Science Reviews. 186: 78–90. Bibcode:2018QSRv..186...78R. doi:10.1016/j.quascirev.2018.02.015. ISSN 0277-3791. The initial source where this map comes from had the map caption the wrong way around: Wang, Xinming; Wang, Yuhong; Chen, Liqi; Sun, Liguang; Wang, Jianjun (10 June 2016). "The abrupt climate change near 4,400 yr BP on the cultural transition in Yuchisi, China and its global linkage". Scientific Reports. 6: 27723. Bibcode:2016NatSR...627723W. doi:10.1038/srep27723. ISSN 2045-2322. PMC 4901284. PMID 27283832.
  2. ^ a b c Roland, Thomas P.; et al. (2014). "Was there a '4.2 ka event' in Great Britain and Ireland? Evidence from the peatland record" (PDF). Quaternary Science Reviews. 83: 11–27. Bibcode:2014QSRv...83...11R. doi:10.1016/j.quascirev.2013.10.024. hdl:10871/30630.
  3. ^ a b deMenocal, Peter B. (2001). "Cultural Responses to Climate Change During the Late Holocene". Science. 292 (5517): 667–673. Bibcode:2001Sci...292..667D. doi:10.1126/science.1059827. PMID 11303088. S2CID 18642937.
  4. ^ Gibbons, Ann (1993). "How the Akkadian Empire Was Hung Out to Dry". Science. 261 (5124): 985. Bibcode:1993Sci...261..985G. doi:10.1126/science.261.5124.985. PMID 17739611.
  5. ^ Li, Chun-Hai; Li, Yong-Xiang; Zheng, Yun-Fei; Yu, Shi-Yong; Tang, Ling-Yu; Li, Bei-Bei; Cui, Qiao-Yu (August 2018). "A high-resolution pollen record from East China reveals large climate variability near the Northgrippian-Meghalayan boundary (around 4200 years ago) exerted societal influence". Palaeogeography, Palaeoclimatology, Palaeoecology. 512: 156–165. Bibcode:2018PPP...512..156L. doi:10.1016/j.palaeo.2018.07.031. ISSN 0031-0182. S2CID 133896325.
  6. ^ a b c Staubwasser, M.; et al. (2003). "Climate change at the 4.2 ka BP termination of the Indus valley civilization and Holocene south Asian monsoon variability". Geophysical Research Letters. 30 (8): 1425. Bibcode:2003GeoRL..30.1425S. doi:10.1029/2002GL016822. S2CID 129178112.
  7. ^ a b c Kochhar, Rajesh (2017-07-25). "The Aryan chromosome". The Indian Express. Retrieved 2023-12-19.
  8. ^ a b Voosen, Paul (August 8, 2018). "Massive drought or myth? Scientists spar over an ancient climate event behind our new geological age". Science. Retrieved 9 January 2020.
  9. ^ Yan, Mi; Liu, Jian (21 February 2019). "Physical processes of cooling and mega-drought during the 4.2 ka BP event: results from TraCE-21ka simulations". Climate of the Past. 15 (1): 265–277. Bibcode:2019CliPa..15..265Y. doi:10.5194/cp-15-265-2019. Retrieved 29 August 2023.
  10. ^ Ning, Liang; Liu, Jian; Bradley, Raymond S.; Yan, Mi (10 January 2019). "Comparing the spatial patterns of climate change in the 9th and 5th millennia BP from TRACE-21 model simulations". Climate of the Past. 15 (1): 41–52. Bibcode:2019CliPa..15...41N. doi:10.5194/cp-15-41-2019. Retrieved 29 August 2023.
  11. ^ Jalali, Bassem; Sicre, Marie-Alexandrine; Azuara, Julien; Pellichero, Violaine; Combourieu-Nebout, Nathalie (8 April 2019). "Influence of the North Atlantic subpolar gyre circulation on the 4.2 ka BP event". Climate of the Past. 15 (2): 701–711. Bibcode:2019CliPa..15..701J. doi:10.5194/cp-15-701-2019. Retrieved 29 August 2023.
  12. ^ Bini, Monica; Zanchetta, Giovanni; Perşoiu, Aurel; Carter, Rosine; Català, Albert; Cacho, Isabel; Dean, Jonathan R.; Di Bine, Federico; Drysdale, Russell N.; Finnè, Martin; Isola, Ilaria; Jalali, Bassem; Lirer, Fabrizio; Magri, Donatella; Massi, Alessia; Marks, Leszek; Mercuri, Anna Maria; Peyron, Odile; Satori, Laura; Sicre, Marie-Alexandrine; Welc, Fabian; Zielhofer, Christoph; Brisset, Elodie (27 March 2019). "The 4.2 ka BP Event in the Mediterranean region: an overview". Climate of the Past. 15 (2): 555–577. Bibcode:2019CliPa..15..555B. doi:10.5194/cp-15-555-2019. Retrieved 29 August 2023.
  13. ^ Toth, Lauren T.; Aronson, Richard B. (16 January 2019). "The 4.2 ka event, ENSO, and coral reef development". Climate of the Past. 15 (1): 105–119. Bibcode:2019CliPa..15..105T. doi:10.5194/cp-15-105-2019. Retrieved 29 August 2023.
  14. ^ Bradley, Raymond S.; Bakke, Jostein (2 September 2019). "Is there evidence for a 4.2 ka BP event in the northern North Atlantic region?". Climate of the Past. 15 (5): 1665–1676. Bibcode:2019CliPa..15.1665B. doi:10.5194/cp-15-1665-2019. Retrieved 29 August 2023.
  15. ^ a b Geirsdóttir, Áslaug; Miller, Gifford H.; Andrews, John T.; Harning, David J.; Anderson, Leif S.; Florian, Christopher; Larsen, Darren J.; Thordarson, Thor (8 January 2019). "The onset of neoglaciation in Iceland and the 4.2 ka event". Climate of the Past. 15 (1): 25–40. Bibcode:2019CliPa..15...25G. doi:10.5194/cp-15-25-2019. Retrieved 29 August 2023.
  16. ^ Gasse, Françoise; Van Campo, Elise (1994). "Abrupt post-glacial climate events in West Asia and North Africa monsoon domains". Earth and Planetary Science Letters. 126 (4): 435–456. Bibcode:1994E&PSL.126..435G. doi:10.1016/0012-821X(94)90123-6.
  17. ^ Bar-Matthews, Miryam; Ayalon, Avner; Kaufman, Aaron (1997). "Late Quaternary Paleoclimate in the Eastern Mediterranean Region from Stable Isotope Analysis of Speleothems at Soreq Cave, Israel". Quaternary Research. 47 (2): 155–168. Bibcode:1997QuRes..47..155B. doi:10.1006/qres.1997.1883. S2CID 128577967.
  18. ^ Arz, Helge W.; et al. (2006). "A pronounced dry event recorded around 4.2 ka in brine sediments from the northern Red Sea". Quaternary Research. 66 (3): 432–441. Bibcode:2006QuRes..66..432A. doi:10.1016/j.yqres.2006.05.006. S2CID 55910028.
  19. ^ a b Parker, Adrian G.; et al. (2006). "A record of Holocene climate change from lake geochemical analyses in southeastern Arabia" (PDF). Quaternary Research. 66 (3): 465–476. Bibcode:2006QuRes..66..465P. doi:10.1016/j.yqres.2006.07.001. S2CID 140158532. Archived from the original (PDF) on October 29, 2008.
  20. ^ Booth, Robert K.; et al. (2005). "A severe centennial-scale drought in midcontinental North America 4200 years ago and apparent global linkages". The Holocene. 15 (3): 321–328. Bibcode:2005Holoc..15..321B. doi:10.1191/0959683605hl825ft. S2CID 39419698.
  21. ^ Menounos, B.; et al. (2008). "Western Canadian glaciers advance in concert with climate change c. 4.2 ka". Geophysical Research Letters. 35 (7): L07501. Bibcode:2008GeoRL..35.7501M. doi:10.1029/2008GL033172. S2CID 13069875.
  22. ^ Drysdale, Russell; et al. (2005). "Late Holocene drought responsible for the collapse of Old World civilizations is recorded in an Italian cave flowstone". Geology. 34 (2): 101–104. Bibcode:2006Geo....34..101D. doi:10.1130/G22103.1.
  23. ^ Thompson, L. G.; et al. (2002). "Kilimanjaro Ice Core Records Evidence of Holocene Climate Change in Tropical Africa". Science. 298 (5593): 589–93. Bibcode:2002Sci...298..589T. doi:10.1126/science.1073198. PMID 12386332. S2CID 32880316.
  24. ^ Davis, Mary E.; Thompson, Lonnie G. (2006). "An Andean ice-core record of a Middle Holocene mega-drought in North Africa and Asia". Annals of Glaciology. 43 (1): 34–41. Bibcode:2006AnGla..43...34D. doi:10.3189/172756406781812456.
  25. ^ Bond, G.; et al. (1997). "A Pervasive Millennial-Scale Cycle in North Atlantic Holocene and Glacial Climates" (PDF). Science. 278 (5341): 1257–1266. Bibcode:1997Sci...278.1257B. doi:10.1126/science.278.5341.1257. S2CID 28963043. Archived from the original (PDF) on 2008-02-27.
  26. ^ "Two examples of abrupt climate change". Lamont–Doherty Earth Observatory. Archived from the original on 2007-08-23.
  27. ^ "Meghalaya Age: Newest phase in Earth's history named after Meghalaya rock | – Times of India". The Times of India. 19 July 2018.
  28. ^ Amos, Jonathan (18 July 2018). "Welcome to the Meghalayan Age a new phase in history". BBC News.
  29. ^ "Collapse of civilizations worldwide defines youngest unit of the Geologic Time Scale".
  30. ^ "Formal subdivision of the Holocene Series/Epoch" (PDF).
  31. ^ Swindles, Graeme T.; Lawson, Ian T.; Matthews, Ian P.; Blaauw, Maarten; Daley, Timothy J.; Charman, Dan J.; Roland, Thomas P.; Plunkett, Gill; Schettler, Georg; Gearey, Benjamin R.; Turner, T. Edward; Rea, Heidi A.; Roe, Helen M.; Amesbury, Matthew J.; Chambers, Frank M.; Holmes, Jonathan; Mitchell, Fraser J. G.; Blackford, Jeffrey; Blundell, Antony; Branch, Nicholas; Holmes, Jane; Langdon, Peter; McCarroll, Julia; McDermott, Frank; Oksanen, Pirita O.; Pritchard, Oliver; Stastney, Phil; Stefanini, Bettina; Young, Dan; Wheeler, Jane; Becker, Katharina; Armit, Ian (November 2013). "Centennial-scale climate change in Ireland during the Holocene". Earth-Science Reviews. 126: 300–320. Bibcode:2013ESRv..126..300S. doi:10.1016/j.earscirev.2013.08.012. S2CID 52248969. Retrieved 18 March 2023.
  32. ^ Bebchuk, Tatiana; Krusic, Paul J.; Pike, Joshua H.; Piermattei, Alma; Friedrich, Ronny; Wacker, Lukas; Crivellaro, Alan; Arosio, Tito; Kirdyanov, Alexander V.; Gibbard, Philip; Brown, David; Esper, Jan; Reinig, Frederick; Büntgen, Ulf (November 2023). "Sudden disappearance of yew (Taxus baccata) woodlands from eastern England coincides with a possible climate event around 4.2 ka ago". Quaternary Science Reviews. 323: 108414. doi:10.1016/j.quascirev.2023.108414. Retrieved 26 December 2023 – via ResearchGate.
  33. ^ Pleskot, Krzysztof; Apolinarska, Karina; Kołaczek, Piotr; Suchora, Magdalena; Fojutowski, Michał; Joniak, Tomasz; Kotrys, Bartosz; Kramkowski, Mateusz; Słowiński, Michał; Woźniak, Magdalena; Lamentowicz, Mariusz (August 2020). "Searching for the 4.2 ka climate event at Lake Spore, Poland". CATENA. 191: 104565. Bibcode:2020Caten.19104565P. doi:10.1016/j.catena.2020.104565. S2CID 216227365.
  34. ^ Schirrmacher, Julien; Weinelt, Mara; Blanz, Thomas; Andersen, Nils; Salgueiro, Emília; Schneider, Ralph R. (2 April 2019). "Multi-decadal atmospheric and marine climate variability in southern Iberia during the mid- to late-Holocene". Climate of the Past. 15 (2): 617–634. Bibcode:2019CliPa..15..617S. doi:10.5194/cp-15-617-2019. Retrieved 29 August 2023.
  35. ^ Mejías Moreno, M., Benítez de Lugo Enrich, L., Pozo Tejado, J. del y Moraleda Sierra, J. 2014. "Los primeros aprovechamientos de aguas subterráneas en la Península Ibérica. Las motillas de Daimiel en la Edad del Bronce de La Mancha". Boletín Geológico y Minero, 125 (4): 455–474 ISSN 0366-0176
  36. ^ Isola, Ilaria; Zanchetta, Giovanni; Drysdale, Russell N.; Regattieri, Eleonora; Bini, Monica; Bajo, Petra; Hellstrom, John C.; Baneschi, Ilaria; Lionello, Piero; Woodhead, Jon; Greig, Alan (22 January 2019). "The 4.2 ka event in the central Mediterranean: new data from a Corchia speleothem (Apuan Alps, central Italy)". Climate of the Past. 15 (1): 135–151. Bibcode:2019CliPa..15..135I. doi:10.5194/cp-15-135-2019. Retrieved 29 August 2023.
  37. ^ a b Zanchetta, Giovanni; Regattieri, Eleonora; Isola, Ilaria; Drysdale, Russell N.; Baneschi, Ilaria; Hellstrom, John C. (18 October 2021). "THE SO-CALLED "4.2 EVENT" IN THE CENTRAL MEDITERRANEAN AND ITS CLIMATIC TELECONNECTIONS". Alpine and Mediterranean Quaternary. 29 (1): 5–17. ISSN 2279-7335. Retrieved 3 September 2023.
  38. ^ Carter, Rosine; Sylvestre, Florence; Paillès, Christine; Sonzogni, Corinne; Couapel, Martine; Alexandre, Anne; Mazur, Jean-Charles; Brisset, Elodie; Miramont, Cécile; Guiter, Frédéric (7 February 2019). "Diatom-oxygen isotope record from high-altitude Lake Petit (2200 m a.s.l.) in the Mediterranean Alps: shedding light on a climatic pulse at 4.2 ka". Climate of the Past. 15 (1): 253–263. Bibcode:2019CliPa..15..253C. doi:10.5194/cp-15-253-2019. Retrieved 29 August 2023.
  39. ^ Di Rita, Federico; Magri, Donatella (7 February 2019). "The 4.2 ka event in the vegetation record of the central Mediterranean". Climate of the Past. 15 (1): 237–251. Bibcode:2019CliPa..15..237D. doi:10.5194/cp-15-237-2019. Retrieved 29 August 2023.
  40. ^ Zielhofer, Christoph; Köhler, Anne; Mischke, Steffen; Benkaddour, Abdelfattah; Mikdad, Abdeslam; Fletcher, William J. (20 March 2019). "Western Mediterranean hydro-climatic consequences of Holocene ice-rafted debris (Bond) events". Climate of the Past. 15 (2): 463–475. Bibcode:2019CliPa..15..463Z. doi:10.5194/cp-15-463-2019. Retrieved 29 August 2023.
  41. ^ Stanley, Jean-Daniel; et al. (2003). "Nile flow failure at the end of the Old Kingdom, Egypt: Strontium isotopic and petrologic evidence". Geoarchaeology. 18 (3): 395–402. doi:10.1002/gea.10065. S2CID 53571037.
  42. ^ Kaniewski, David; Marriner, Nick; Cheddadi, Rachid; Guiot, Joël; Van Campo, Elise (22 October 2018). "The 4.2 ka BP event in the Levant". Climate of the Past. 14 (10): 1529–1542. Bibcode:2018CliPa..14.1529K. doi:10.5194/cp-14-1529-2018. Retrieved 29 August 2023.
  43. ^ Carolin, Stacy A.; Walker, Richard T.; Day, Christopher C.; Ersek, Vasile; Sloan, R. Alastair; Dee, Michael W.; Talebian, Morteza; Henderson, Gideon M. (24 December 2018). "Precise timing of abrupt increase in dust activity in the Middle East coincident with 4.2 ka social change". Proceedings of the National Academy of Sciences of the United States of America. 116 (1): 67–72. doi:10.1073/pnas.1808103115. ISSN 0027-8424. PMC 6320537. PMID 30584111.
  44. ^ Cullen, Heidi M.; deMenocal, Peter B. (2000). "North Atlantic influence on Tigris-Euphrates streamflow". International Journal of Climatology. 20 (8): 853–863. Bibcode:2000IJCli..20..853C. doi:10.1002/1097-0088(20000630)20:8<853::AID-JOC497>3.0.CO;2-M.
  45. ^ Kerr, Richard A. (1998). "Sea-Floor Dust Shows Drought Felled Akkadian Empire". Science. 279 (5349): 325–326. Bibcode:1998Sci...279..325K. doi:10.1126/science.279.5349.325. S2CID 140563513.
  46. ^ Cullen, H. M. et al., "Climate change and the collapse of the Akkadian empire: Evidence from the deep sea", Geology, vol. 28, iss. 4, pp. 379–382, 2000
  47. ^ a b c Weiss, H.; et al. (1993). "The Genesis and Collapse of Third Millennium North Mesopotamian Civilization". Science. 261 (5124): 995–1004. Bibcode:1993Sci...261..995W. doi:10.1126/science.261.5124.995. PMID 17739617. S2CID 31745857.
  48. ^ Danti, Michael (8 November 2010). "Late Middle Holocene Climate and Northern Mesopotamia: Varying Cultural Responses to the 5.2 and 4.2 ka Aridification Events". In Mainwaring, A. Bruce; Giegengack, Robert; Vita-Finzi, Claudio (eds.). Climate Crises in Human History. American Philosophical Society. pp. 139–172. ISBN 9781606189214. Retrieved 3 September 2023.
  49. ^ Riehl, S. (2008). "Climate and agriculture in the ancient Near East: a synthesis of the archaeobotanical and stable carbon isotope evidence". Vegetation History and Archaeobotany. 17 (1): 43–51. Bibcode:2008VegHA..17S..43R. doi:10.1007/s00334-008-0156-8. S2CID 128622745.
  50. ^ Burke, Aaron A. (2021). The Amorites and the Bronze Age Near East: The Making of a Regional Identity. Cambridge University Press. ISBN 9781108495967.
  51. ^ Watanabe, Takaaki K.; Watanabe, Tsuyoshi; Yamazaki, Atsuko; Pfeiffer, Miriam (2019). "Oman corals suggest that a stronger winter shamal season caused the Akkadian Empire (Mesopotamia) collapse". Geology. 47 (12). GeoScienceWorld: 1141–1145. Bibcode:2019Geo....47.1141W. doi:10.1130/G46604.1. S2CID 204781389.
  52. ^ "Strong winter dust storms may have caused the collapse of the Akkadian Empire". Hokkaido University. 24 October 2019.
  53. ^ Perşoiu, Aurel; Ionita, Monica; Weiss, Harvey (11 April 2019). "Atmospheric blocking induced by the strengthened Siberian High led to drying in west Asia during the 4.2 ka BP event – a hypothesis". Climate of the Past. 15 (2): 781–793. Bibcode:2019CliPa..15..781P. doi:10.5194/cp-15-781-2019. Retrieved 29 August 2023.
  54. ^ Giesche, Alena; Staubwasser, Michael; Petrie, Cameron A.; Hodell, David A. (15 January 2019). "Indian winter and summer monsoon strength over the 4.2 ka BP event in foraminifer isotope records from the Indus River delta in the Arabian Sea". Climate of the Past. 15 (1): 73–90. Bibcode:2019CliPa..15...73G. doi:10.5194/cp-15-73-2019. Retrieved 29 August 2023.
  55. ^ Nakamura, Atsunori; Yokoyama, Yusuke; Maemoku, Hideaki; Yagi, Hiroshi; Okamura, Makoto; Matsuoka, Hiromi; Miyake, Nao; Osada, Toshiki; Adhikari, Danda Pani; Dangol, Vishnu; Ikehara, Minoru; Miyairi, Yosuke; Matsuzaki, Hiroyuki (18 March 2016). "Weak monsoon event at 4.2 ka recorded in sediment from Lake Rara, Himalayas". Quaternary International. Japanese Quaternary Studies. 397: 349–359. Bibcode:2016QuInt.397..349N. doi:10.1016/j.quaint.2015.05.053. ISSN 1040-6182. Retrieved 8 September 2023.
  56. ^ Mehrotra, Nivedita; Shah, Santosh K.; Basavaiah, Nathani; Laskar, Amzad H.; Yadava, Madhusudan G. (25 February 2019). "Resonance of the '4.2ka event' and terminations of global civilizations during the Holocene, in the palaeoclimate records around PT Tso Lake, Eastern Himalaya". Quaternary International. Holocene Civilization. 507: 206–216. Bibcode:2019QuInt.507..206M. doi:10.1016/j.quaint.2018.09.027. ISSN 1040-6182. S2CID 135417137. Retrieved 8 September 2023.
  57. ^ Kathayat, Gayatri; Cheng, Hai; Sinha, Ashish; Berkelhammer, Max; Zhang, Haiwei; Duan, Pengzhen; Li, Hanying; Li, Xianglei; Ning, Youfeng; Edwards, Robert Lawrence (13 November 2018). "Evaluating the timing and structure of the 4.2 ka event in the Indian summer monsoon domain from an annually resolved speleothem record from Northeast India". Climate of the Past. 14 (12): 1869–1879. doi:10.5194/cp-14-1869-2018. Retrieved 29 August 2023.
  58. ^ Giesche, Alena; Hodell, David A.; Petrie, Cameron A.; Haug, Gerald H.; Adkins, Jess F.; Plessen, Birgit; Marwan, Norbert; Bradbury, Harold J.; Hartland, Adam; French, Amanda D.; Breitenbach, Sebastian F. M. (4 April 2023). "Recurring summer and winter droughts from 4.2-3.97 thousand years ago in north India". Communications Earth & Environment. 4 (1): 103. Bibcode:2023ComEE...4..103G. doi:10.1038/s43247-023-00763-z. ISSN 2662-4435. S2CID 257915185. Retrieved 8 September 2023.
  59. ^ a b c Demkina, T. S. (2017). "Paleoecological crisis in the steppes of the Lower Volga region in the Middle of the Bronze Age (III–II centuries BC)". Eurasian Soil Science. 50 (7): 791–804. Bibcode:2017EurSS..50..791D. doi:10.1134/S1064229317070018. S2CID 133638705.
  60. ^ "Decline of Bronze Age 'megacities' linked to climate change". phys.org.
  61. ^ Lawler, Andrew (6 June 2008). "Indus Collapse: The End or the Beginning of an Asian Culture?". Science. 320 (5881): 1282–1283. doi:10.1126/science.320.5881.1281. PMID 18535222. S2CID 206580637.
  62. ^ a b c Giosan, L.; et al. (2012). "Fluvial landscapes of the Harappan Civilization". Proceedings of the National Academy of Sciences of the United States of America. 109 (26): E1688–E1694. Bibcode:2012PNAS..109E1688G. doi:10.1073/pnas.1112743109. PMC 3387054. PMID 22645375.
  63. ^ Clift et al., 2011, "U–Pb zircon dating evidence for a Pleistocene Sarasvati River and capture of the Yamuna River", Geology, 40, 211–214 (2011).
  64. ^ Tripathi, Jayant K.; Tripathi, K.; Bock, Barbara; Rajamani, V. & Eisenhauer, A. (25 October 2004). "Is River Ghaggar, Saraswati? Geochemical Constraints" (PDF). Current Science. 87 (8).
  65. ^ Nuwer, Rachel (28 May 2012). "An Ancient Civilization, Upended by Climate Change". LiveScience. Retrieved 29 May 2012.
  66. ^ Choi, Charles (29 May 2012). "Huge Ancient Civilization's Collapse Explained". The New York Times. Retrieved 18 May 2016.
  67. ^ Madella, Marco; Fuller, Dorian (2006). "Palaeoecology and the Harappan Civilisation of South Asia: a reconsideration". Quaternary Science Reviews. 25 (11–12): 1283–1301. Bibcode:2006QSRv...25.1283M. doi:10.1016/j.quascirev.2005.10.012.
  68. ^ MacDonald, Glen (2011). "Potential influence of the Pacific Ocean on the Indian summer monsoon and Harappan decline". Quaternary International. 229 (1–2): 140–148. Bibcode:2011QuInt.229..140M. doi:10.1016/j.quaint.2009.11.012.
  69. ^ Brooke, John L. (2014), Climate Change and the Course of Global History: A Rough Journey, Cambridge University Press, p. 296, Bibcode:2014cccg.book.....B, ISBN 978-0-521-87164-8
  70. ^ a b c Xiao, Jule; Zhang, Shengrui; Fan, Jiawei; Wen, Ruilin; Zhai, Dayou; Tian, Zhiping; Jiang, Dabang (11 October 2018). "The 4.2 ka BP event: multi-proxy records from a closed lake in the northern margin of the East Asian summer monsoon". Climate of the Past. 14 (10): 1417–1425. Bibcode:2018CliPa..14.1417X. doi:10.5194/cp-14-1417-2018. Retrieved 29 August 2023.
  71. ^ Kaboth-Bahr, Stefanie; Bahr, André; Zeeden, Christian A.; Yamoah, Kweku A.; Lone, Mahjoor Ahmad; Chuang, Chih-Kai; Löwemark, Ludvig; Wei, Kuo-Yen (25 March 2021). "A tale of shifting relations: East Asian summer and winter monsoon variability during the Holocene". Scientific Reports. 11 (1): 6938. Bibcode:2021NatSR..11.6938K. doi:10.1038/s41598-021-85444-7. PMC 7994397. PMID 33767210.
  72. ^ Zhang, Haiwei; Cheng, Hai; Cai, Yanjun; Spötl, Christoph; Kathayat, Gayathri; Sinha, Ashish; Edwards, R. Lawrence; Tan, Liangcheng (27 November 2018). "Hydroclimatic variations in southeastern China during the 4.2 ka event reflected by stalagmite records". Climate of the Past. 14 (11): 1805–1817. doi:10.5194/cp-14-1805-2018. Retrieved 29 August 2023.
  73. ^ Scuderi, Louis A.; Yang, Xiaoping; Ascoli, Samantha E.; Li, Hongwei (21 February 2019). "The 4.2 ka BP Event in northeastern China: a geospatial perspective". Climate of the Past. 15 (1): 367–375. Bibcode:2019CliPa..15..367S. doi:10.5194/cp-15-367-2019. Retrieved 29 August 2023.
  74. ^ Yujie, Bai; Jiangying, Wu; Yijia, Liang; Qingfeng, Shao (30 July 2020). "THE MULTI-PROXY RECORD OF A STALAGMITE FROM YULONG CAVE,HUBEI DURING THE 4.2 KA EVENT". Quaternary Sciences. 40 (4): 959–972. doi:10.11928/j.issn.1001-7410.2020.04.11 (inactive 1 November 2024). Retrieved 3 September 2023.{{cite journal}}: CS1 maint: DOI inactive as of November 2024 (link)
  75. ^ Park, Jungjae; Park, Jinheum; Yi, Sangheon; Kim, Jin Cheul; Lee, Eunmi; Choi, Jieun (25 July 2019). "Abrupt Holocene climate shifts in coastal East Asia, including the 8.2 ka, 4.2 ka, and 2.8 ka BP events, and societal responses on the Korean peninsula". Scientific Reports. 9 (1): 10806. Bibcode:2019NatSR...910806P. doi:10.1038/s41598-019-47264-8. PMC 6658530. PMID 31346228.
  76. ^ 三内丸山遺跡について三内丸山遺跡とは（公式サイト）。
  77. ^ (a) Shuzo Koyama, "Jomon Subsistence and Population", Senri Ethnological Studies no. 2, 1–65 (1978). (b) 小山修三, 『縄文時代』, 中央公論社, 1983. なお『縄文時代』では遺跡数に乗じる係数を、弥生時代57人、縄文時代中期以降24人、縄文時代早期8.5人と紹介しているが、実際の数値計算に合わせ、本文のように修正した。
  78. ^ Leipe, Christian; Müller, Stefanie; Hille, Konrad; Kato, Hirofumi; Kobe, Franziska; Schmidt, Mareike; Seyffert, Konrad; Spengler, Robert; Wagner, Mayke; Weber, Andrzej W.; Tarasov, Pavel E. (1 August 2018). "Vegetation change and human impacts on Rebun Island (Northwest Pacific) over the last 6000 years". Quaternary Science Reviews. 193: 129–144. Bibcode:2018QSRv..193..129L. doi:10.1016/j.quascirev.2018.06.011. ISSN 0277-3791. Retrieved 8 September 2023.
  79. ^ Wu, Wenxiang; Liu, Tungsheng (2004). "Possible role of the "Holocene Event 3" on the collapse of Neolithic Cultures around the Central Plain of China". Quaternary International. 117 (1): 153–166. Bibcode:2004QuInt.117..153W. doi:10.1016/S1040-6182(03)00125-3.
  80. ^ Chun Chang Huang; et al. (2011). "Extraordinary floods related to the climatic event at 4200 a BP on the Qishuihe River, middle reaches of the Yellow River, China". Quaternary Science Reviews. 30 (3–4): 460–468. Bibcode:2011QSRv...30..460H. doi:10.1016/j.quascirev.2010.12.007.
  81. ^ Gao, Huazhong; Zhu, Cheng; Xu, Weifeng (2007). "Environmental change and cultural response around 4200 cal. yr BP in the Yishu River Basin, Shandong". Journal of Geographical Sciences. 17 (3): 285–292. Bibcode:2007JGSci..17..285G. doi:10.1007/s11442-007-0285-5. S2CID 186227589.
  82. ^ "Migration of the Tribe and Integration into the Han Chinese". Qingpu Museum. Archived from the original on 2016-03-04. Retrieved 29 January 2014.
  83. ^ Wang, Jianjun; Sun, Liguang; Chen, Liqi; Xu, Libin; Wang, Yuhong; Wang, Xinming (10 June 2016). "The abrupt climate change near 4,400 yr BP on the cultural transition in Yuchisi, China and its global linkage". Scientific Reports. 6 (1): 27723. Bibcode:2016NatSR...627723W. doi:10.1038/srep27723. ISSN 2045-2322. PMC 4901284. PMID 27283832.
  84. ^ Leipe, C.; Long, T.; Sergusheva, E. A.; Wagner, M.; Tarasov, P. E. (6 September 2019). "Discontinuous spread of millet agriculture in eastern Asia and prehistoric population dynamics". Science Advances. 5 (9): eaax6225. Bibcode:2019SciA....5.6225L. doi:10.1126/sciadv.aax6225. ISSN 2375-2548. PMC 6760930. PMID 31579827.
  85. ^ Railsback, L. Bruce; Liang, Fuyuan; Brook, George A.; Cheng, Hai; Edwards, R. Lawrence (15 January 2022). "Additional multi-proxy stalagmite evidence from northeast Namibia supports recent models of wetter conditions during the 4.2 ka Event in the Southern Hemisphere". Palaeogeography, Palaeoclimatology, Palaeoecology. 586: 110756. Bibcode:2022PPP...58610756R. doi:10.1016/j.palaeo.2021.110756. S2CID 244126683. Retrieved 3 September 2023.
  86. ^ Railsback, L. Bruce; Liang, Fuyuan; Brook, G.A.; Voarintsoa, Ny Riavo G.; Sletten, Hillary R.; Marais, Eugene; Hardt, Ben; Cheng, Hai; Edwards, R. Lawrence (15 April 2018). "The timing, two-pulsed nature, and variable climatic expression of the 4.2 ka event: A review and new high-resolution stalagmite data from Namibia". Quaternary Science Reviews. 186: 78–90. Bibcode:2018QSRv..186...78R. doi:10.1016/j.quascirev.2018.02.015. Retrieved 3 September 2023.
  87. ^ Li, Hanying; Cheng, Hai; Sinha, Ashish; Kathayat, Gayatri; Spötl, Christoph; André, Aurèle Anquetil; Meunier, Arnaud; Biswas, Jayant; Duan, Pengzhen; Ning, Youfeng; Edwards, Richard Lawrence (7 December 2018). "Hydro-climatic variability in the southwestern Indian Ocean between 6000 and 3000 years ago". Climate of the Past. 14 (12): 1881–1891. Bibcode:2018CliPa..14.1881L. doi:10.5194/cp-14-1881-2018. Retrieved 29 August 2023.

Further reading

source: https://en.wikipedia.org/wiki/4.2-kiloyear_event