Monsoon - Knowledge

950:, the July ITCZ, the zone of rainfall maximum, migrated northwards, increasing precipitation over southern China during the East Asian Summer Monsoon (EASM) while making Indochina drier. During the Late Miocene Global Cooling (LMCG), from 7.9 to 5.8 million years ago, the East Asian Winter Monsoon (EAWM) became stronger as the subarctic front shifted southwards. An abrupt intensification of the EAWM occurred 5.5 million years ago. The EAWM was still significantly weaker relative to today between 4.3 and 3.8 million years ago but abruptly became more intense around 3.8 million years ago as crustal stretching widened the Tsushima Strait and enabled greater inflow of the warm Tsushima Current into the Sea of Japan. Circa 3.0 million years ago, the EAWM became more stable, having previously been more variable and inconsistent, in addition to being enhanced further amidst a period of global cooling and sea level fall. The EASM was weaker during cold intervals of glacial periods such as the 962:. The EASM expanded its influence deeper into the interior of Asia as sea levels rose following the LGM; it also underwent a period of intensification during the Middle Holocene, around 6,000 years ago, due to orbital forcing made more intense by the fact that the Sahara at the time was much more vegetated and emitted less dust. This Middle Holocene interval of maximum EASM was associated with an expansion of temperate deciduous forest steppe and temperate mixed forest steppe in northern China. By around 5,000 to 4,500 BP, the East Asian monsoon's strength began to wane, weakening from that point until the present day. A particularly notable weakening took place ~3,000 BP. The location of the EASM shifted multiple times over the course of the Holocene: first, it moved southward between 12,000 and 8,000 BP, followed by an expansion to the north between approximately 8,000 and 4,000 BP, and most recently retreated southward once more between 4,000 and 0 BP. 2101: 2109: 52: 1821: 2016: 1992: 1681: 1019: 1033: 1619: 4920: 693: 40: 2179: 829: 1983: 1054: 2277:) is the result of a resurgence of westerly winds from the Atlantic, where they become loaded with wind and rain. These westerly winds are a common phenomenon during the European winter, but they ease as spring approaches in late March and through April and May. The winds pick up again in June, which is why this phenomenon is also referred to as "the return of the westerlies". 1081:

according to the land–sea heating contrast and it is thought that the northern extent of the monsoon in South Asia is influenced by the high Tibetan Plateau. These temperature imbalances happen because oceans and land absorb heat in different ways. Over oceans, the air temperature remains relatively stable for two reasons: water has a relatively high

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caused by higher temperature over land than in the ocean. This is no longer considered as the cause and the monsoon is now considered a planetary-scale phenomenon involving the annual migration of the Intertropical Convergence Zone between its northern and southern limits. The limits of the ITCZ vary

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closed. When this happened, cold waters in the Pacific were impeded from flowing into the Indian Ocean. It is believed that the resulting increase in sea surface temperatures in the Indian Ocean increased the intensity of monsoons. In 2018, a study of the SAM's variability over the past million years

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In the colder months, the cycle is reversed. Then the land cools faster than the oceans and the air over the land has higher pressure than air over the ocean. This causes the air over the land to flow to the ocean. When humid air rises over the ocean, it cools, and this causes precipitation over the

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generally warms the Indian Ocean. Thus these five intervals could probably be those of considerable lowering of SST in the Indian Ocean and would have influenced Indian monsoon intensity. During the weak LC, there is the possibility of reduced intensity of the Indian winter monsoon and strong summer

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The rain usually arrives in two waves, at the beginning of June, and again in mid- to late June. The European monsoon is not a monsoon in the traditional sense in that it doesn't meet all the requirements to be classified as such. Instead, the return of the westerlies is more regarded as a conveyor

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periods like the present day. The Indian Summer Monsoon (ISM) underwent several intensifications during the warming following the Last Glacial Maximum, specifically during the time intervals corresponding to 16,100–14,600 BP, 13,600–13,000 BP, and 12,400–10,400 BP as indicated by vegetation changes

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and northern Australia (December, January). However, the monsoon is not a simple response to heating but a more complex interaction of topography, wind and sea, as demonstrated by its abrupt rather than gradual withdrawal from the region. The Australian monsoon (the "Wet") occurs in the southern

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Most summer monsoons have a dominant westerly component and a strong tendency to ascend and produce copious amounts of rain (because of the condensation of water vapor in the rising air). The intensity and duration, however, are not uniform from year to year. Winter monsoons, by contrast, have a

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and adjoining areas of the northern and central Indian subcontinent heat up considerably during the hot summers. This causes a low pressure area over the northern and central Indian subcontinent. To fill this void, the moisture-laden winds from the Indian Ocean rush into the subcontinent. These

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Around September, with the sun retreating south, the northern landmass of the Indian subcontinent begins to cool off rapidly, and air pressure begins to build over northern India. The Indian Ocean and its surrounding atmosphere still hold their heat, causing cold wind to sweep down from the

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will equilibrate a hot or cold surface with deeper water (up to 50 metres). In contrast, dirt, sand, and rocks have lower heat capacities (0.19 to 0.35 J g K), and they can only transmit heat into the earth by conduction and not by convection. Therefore, bodies of water stay at a more even

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topography towards Australia. This forms a cyclonic circulation vortex over Borneo, which together with descending cold surges of winter air from higher latitudes, cause significant weather phenomena in the region. Examples are the formation of a rare low-latitude tropical storm in 2001,

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The monsoon is widely welcomed and appreciated by city-dwellers as well, for it provides relief from the climax of summer heat in June. However, the roads take a battering every year. Often houses and streets are waterlogged and slums are flooded despite drainage systems. A lack of city

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Similar rainfall is caused when moist ocean air is lifted upwards by mountains, surface heating, convergence at the surface, divergence aloft, or from storm-produced outflows at the surface. However the lifting occurs, the air cools due to expansion in lower pressure, and this produces

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in the Tibetan Plateau displaying increases in humidity brought by an intensifying ISM. Though the ISM was relatively weak for much of the Late Holocene, significant glacial accumulation in the Himalayas still occurred due to cold temperatures brought by westerlies from the west.

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The onset of the summer monsoon is marked by a period of premonsoonal rain over South China and Taiwan in early May. From May through August, the summer monsoon shifts through a series of dry and rainy phases as the rain belt moves northward, beginning over

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to blow from the ocean to the land, bringing moist air inland. This moist air rises to a higher altitude over land and then it flows back toward the ocean (thus completing the cycle). However, when the air rises, and while it is still over the land, the air

2136:. It is characterised by a warm, rainy summer monsoon and a cold, dry winter monsoon. The rain occurs in a concentrated belt that stretches east–west except in East China where it is tilted east-northeast over Korea and Japan. The seasonal rain is known as 1755:

of Southern California, but rarely reaches the coastal strip (a wall of desert thunderstorms only a half-hour's drive away is a common summer sight from the sunny skies along the coast during the monsoon). The North American monsoon is known to many as the

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The Asian monsoons may be classified into a few sub-systems, such as the Indian Subcontinental Monsoon which affects the Indian subcontinent and surrounding regions including Nepal, and the East Asian Monsoon which affects southern China,

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Although the North American monsoon region experiences pronounced precipitation seasonally, it differs from a true monsoon, which is characterized by a distinct seasonal reversal of prevailing surface winds. No such situation occurs in

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belt that delivers a series of low-pressure centres to Western Europe where they create unsettled weather. These storms generally feature significantly lower-than-average temperatures, fierce rain or hail, thunder, and strong winds.

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The monsoon accounts for nearly 80% of the rainfall in India. Indian agriculture (which accounts for 25% of the GDP and employs 70% of the population) is heavily dependent on the rains, for growing crops especially like

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at a rate of roughly 1–2 weeks per state, pouring rain all along its way. June 1 is regarded as the date of onset of the monsoon in India, as indicated by the arrival of the monsoon in the southernmost state of Kerala.

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and the equatorial Atlantic Ocean. The ITCZ migrates northward from the equatorial Atlantic in February, reaches western Africa on or near June 22, then moves back to the south by October. The dry, northeasterly

954:(LGM) and stronger during interglacials and warm intervals of glacial periods. Another EAWM intensification event occurred 2.6 million years ago, followed by yet another one around 1.0 million years ago. During 3685:

D. K. Sinha; A. K. Singh & M. Tiwari (2006-05-25). "Palaeoceanographic and palaeoclimatic history of ODP site 763A (Exmouth Plateau), South-east Indian Ocean: 2.2 Ma record of planktic foraminifera".

1879:) with precipitation on coastal areas, west of the Western Ghats. The eastern areas of the Western Ghats do not receive much rain from this monsoon as the wind does not cross the Western Ghats. 1097:

During warmer months sunlight heats the surfaces of both land and oceans, but land temperatures rise more quickly. As the land's surface becomes warmer, the air above it expands and an area of

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The southwest monsoon is generally expected to begin around the beginning of June and fade away by the end of September. The moisture-laden winds on reaching the southernmost point of the

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Zhisheng, An; Kutzbach, John E.; Prell, Warren L.; Porter, Stephen C. (2001). "Evolution of Asian monsoons and phased uplift of the Himalaya–Tibetan plateau since Late Miocene times".

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interglacial, suggests that they had an average duration of around 64 years, with the minimum duration being around 50 years and the maximum approximately 80 years, similar to today.

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The South American summer monsoon (SASM) is known to have become weakened during Dansgaard–Oeschger events. The SASM has been suggested to have been enhanced during Heinrich events.

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and the movement of the heating maxima from the Northern Hemisphere to the Southern Hemisphere. North-easterly winds flow down Southeast Asia, are turned north-westerly/westerly by

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falls during the three summer months, when the region is under the monsoon influence; about 70% of that is directly of "cyclonic" (i.e., monsoon-driven) origin (as opposed to "

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Cheng, Bei; Liu, Jianbao; Chen, Shengqian; Zhang, Zhiping; Shen, Zhongwei; Yan, Xinwei; Li, Fanyi; Chen, Guangjie; Zhang, Xiaosen; Wang, Xin; Chen, Jianhui (5 February 2020).

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A study of marine plankton suggested that the South Asian Monsoon (SAM) strengthened around 5 million years ago. Then, during ice periods, the sea level fell and the

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The January ITCZ migrated further south to its present location during the Middle Miocene, strengthening the summer monsoon of Australia that had previously been weaker.

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of China, many geologists believe the monsoon first became strong around 8 million years ago. More recently, studies of plant fossils in China and new long-duration

1871:, India, thus making this area the first state in India to receive rain from the Southwest Monsoon. This branch of the monsoon moves northwards along the Western Ghats ( 4319: 2378: 2066:

in this region splits into the southern subtropical jet and the polar jet. The subtropical flow directs northeasterly winds to blow across southern Asia, creating dry

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led to a timing of the monsoon beginning 15–20 million years ago and linked to early Tibetan uplift. Testing of this hypothesis awaits deep ocean sampling by the

1715:) occurs from late June or early July into September, originating over Mexico and spreading into the southwest United States by mid-July. It affects Mexico along the 1837:. The Himalayas act like a high wall, blocking the winds from passing into Central Asia, and forcing them to rise. As the clouds rise, their temperature drops, and 4036: 2589:"Initiation of Northern Hemisphere glaciation and strengthening of the northeast Indian monsoon: Ocean Drilling Program Site 758, eastern equatorial Indian Ocean" 1931:

and coarse grains. A delay of a few days in the arrival of the monsoon can badly affect the economy, as evidenced in the numerous droughts in India in the 1990s.

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of a seasonally changing pattern, although technically there is also a dry phase. The term is also sometimes used to describe locally heavy but short-term rains.

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develops. Meanwhile, the ocean remains at a lower temperature than the land, and the air above it retains a higher pressure. This difference in pressure causes

2570: 1951:, also frequently experience heavy floods during this season. Recently, areas in India that used to receive scanty rainfall throughout the year, like the 3359:"Reconstructed moisture evolution of the deserts in northern China since the Last Glacial Maximum and its implications for the East Asian Summer Monsoon" 1935:

infrastructure coupled with changing climate patterns causes severe economic loss including damage to property and loss of lives, as evidenced in the

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due to reduction in net heat input to the Indian Ocean through the Indonesian Throughflow. Thus a better understanding of the possible links between

4062: 1910:, India, is one of the wettest places on Earth. After the arrival at the Eastern Himalayas, the winds turns towards the west, travelling over the 4471: 4368:

Blumer, Felix P. (1998). "Investigations of the precipitation conditions in the central part of the Tianshan mountains". In Kovar, Karel (ed.).

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Wang, Zhenjun; Chen, Shitao; Wang, Yongjin; Cheng, Hai; Liang, Yijia; Yang, Shaohua; Zhang, Zhenqiu; Zhou, Xueqin; Wang, Meng (1 March 2020).

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and Japan (June) and finally to northern China and Korea (July). When the monsoon ends in August, the rain belt moves back to southern China.

4608: 4504: 2410: 4200: 4148: 3925: 2547: 4546: 4233: 2054:, which get less rain from the Southwest Monsoon, receive rain from this Monsoon. About 50% to 60% of the rain received by the state of 1067:

This visualization shows the Asian monsoon and how it develops using observational and modeled data. It also shows some of the impacts.

632: 2920:"Paleoclimatic evolution of the SW and NE South China Sea and its relationship with spectral reflectance data over various age scales" 2803:

Ma, Qingfeng; Zhu, Liping; Lü, Xinmiao; Wang, Junbo; Ju, Jianting; Kasper, Thomas; Daut, Gerhard; Haberzettl, Torsten (March 2019).

2633:"Sixty-year quasi-period of the Asian monsoon around the Last Interglacial derived from an annually resolved stalagmite δ18O record" 3942: 3905: 3881: 3038:"An astronomically tuned 8.1 Ma eolian record from the Chinese Loess Plateau and its implication on the evolution of Asian monsoon" 1970:"). The effects also extend westwards to the Mediterranean, where however the impact of the monsoon is to induce drought via the 4445: 2058:

is from the Northeast Monsoon. In Southern Asia, the northeastern monsoons take place from October to December when the surface

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Extreme difference is very much evident between wet and dry seasons in tropical seasonal forest. The image at left is taken at

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Chen, Xu; McGowan, Suzanne; Xiao, Xiayun; Stevenson, Mark A.; Yang, Xiangdong; Li, Yanling; Zhang, Enlou (1 August 2018).

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Gallagher, Stephen J.; Kitamura, Akihisa; Iryu, Yasufumi; Itaki, Takuya; Koizumi, Itaru; Hoiles, Peter W. (27 June 2015).

981:(PL-1), 1.83 Ma (PL-2), 0.68 Ma (PL-3), 0.45 Ma (PL-4) and 0.04 Ma (PL-5) were identified which showed a weakening of the 4753: 3631:"East Asian summer monsoon and topography co-determine the Holocene migration of forest-steppe ecotone in northern China" 3519:"Direct and indirect effects of Holocene climate variations on catchment and lake processes of a treeline lake, SW China" 622: 4748: 4179: 4656: 4351: 4227: 4033: 1675: 679: 627: 2284:

The return of the westerlies affects Europe's Northern Atlantic coastline, more precisely Ireland, Great Britain, the

4866: 4743: 4728: 4713: 2563: 911: 721: 3249:"Paleoceanographic changes in the East China Sea during the last ~400 kyr reconstructed using planktic foraminifera" 2859:

Peng, Xu; Chen, Yixin; Li, Yingkui; Liu, Beibei; Liu, Qing; Yang, Weilin; Cui, Zhijiu; Liu, Gengnian (April 2020).

782:(ITCZ) between its limits to the north and south of the equator. Usually, the term monsoon is used to refer to the 609: 2567: 3975: 3579: 3042: 2382: 2617: 3463:"Pollen reconstruction and vegetation dynamics of the middle Holocene maximum summer monsoon in northern China" 1651: 1634: 779: 5059: 4768: 4649: 930: 507: 4733: 3312: 2805:"Late glacial and Holocene vegetation and climate variations at Lake Tangra Yumco, central Tibetan Plateau" 955: 3630: 3518: 3462: 3461:

Wang, Wei; Liu, Lina; Li, Yanyan; Niu, Zhimei; He, Jiang; Ma, Yuzhen; Mensing, Scott A. (15 August 2019).

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Gebregiorgis, D.; Hathorne, E. C.; Giosan, L.; Clemens, S.; Nürnberg, D.; Frank, M. (8 November 2018).

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An Erosional Record of the Tibetan Plateau Uplift and Monsoon Strengthening in the Asian Marginal Seas.

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and South American weather patterns with incomplete wind reversal should be counted as true monsoons.

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Liu, Chang; Clift, Peter D.; Giosan, Liviu; Miao, Yunfa; Warny, Sophie; Wan, Shiming (1 July 2019).

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Li, Qin; Wu, Haibin; Yu, Yanyan; Sun, Aizhi; Marković, Slobodan B.; Guo, Zhengtang (October 2014).

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ice ages. A study of Asian monsoonal climate cycles from 123,200 to 121,210 years BP, during the

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The rainy season occurs from September to February and it is a major source of energy for the

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While travelling towards the Indian Ocean, the cold dry wind picks up some moisture from the

1810: 914:. The monsoon has varied significantly in strength since this time, largely linked to global 714: 528: 286: 210: 958:, the EASM grew in strength, but it has been suggested to have decreased in strength during 4636: 4411: 4004:"Southwest Monsoon 2017 Forecast: Warmer-Than-Average Conditions Could Lead to More Storms" 3781: 3644: 3629:

Cheng, Ying; Liu, Hongyan; Dong, Zhibao; Duan, Keqin; Wang, Hongya; Han, Yue (April 2020).

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Piao, Jinling; Chen, Wen; Wang, Lin; Pausata, Francesco S.R.; Zhang, Qiong (January 2020).

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Vats, Nishant; Mishra, Sibasish; Singh, Raj K.; Gupta, Anil K.; Pandey, D. K. (June 2020).

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in central Bangladesh during dry season, and the right one is taken in wet monsoon season.

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and winds are directed toward Australia. In the Philippines, northeast monsoon is called

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dominant easterly component and a strong tendency to diverge, subside and cause drought.

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Igarashi, Yaeko; Irino, Tomohisa; Sawada, Ken; Song, Lu; Furota, Satoshi (April 2018).

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Three-second video of a lightning strike within a thunderstorm over Island in the Sky,

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Ahn, Jinho; Brooks, Edward J.; Schmittner, Andreas; Kreutz, Karl (28 September 2012).

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found that precipitation resulting from the monsoon was significantly reduced during

770:) is traditionally a seasonal reversing wind accompanied by corresponding changes in 543: 4371:

Hydrology, water resources and ecology in headwaters. Volume 248 of IAHS publication

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Kim, Yongmi; Yi, Sangheon; Kim, Gil-Young; Lee, Eunmi; Kong, Sujin (15 April 2019).

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circulation and precipitation associated with annual latitudinal oscillation of the

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Chou, C. (2003). "Land-sea heating contrast in an idealized Asian summer monsoon".

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which produce clear skies over India. Meanwhile, a low pressure system known as a

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Onset dates and prevailing wind currents of the southwest summer monsoons in India

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and Asia around 50 million years ago. Because of studies of records from the

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Ahmad, Latief; Kanth, Raihana Habib; Parvaze, Sabah; Mahdi, Syed Sheraz (2017).

39: 5049: 5034: 4925: 3001: 2771: 2330:. International Geophysics Series. Vol. 15. San Diego, CA: Academic Press. 2113: 2071: 2036: 2020: 1781: 1659: 959: 947: 935: 915: 697: 604: 438: 4034:

Monsoon in West Africa: Classic continuity hides a dual-cycle rainfall regime.

3793: 3749: 3732: 3713: 3407:"Northward extension of the East Asian summer monsoon during the mid-Holocene" 3158: 3133: 2588: 808:

and neighboring countries to refer to the big seasonal winds blowing from the

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Visser, S.W. (1953). Some remarks on the European monsoon. Birkhäuser: Basel.

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Han, Wenxia; Fang, Xiaomin; Berger, André; Yin, Qiuzhen (22 December 2011).

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Proceedings of the Indian Academy of Sciences - Earth and Planetary Sciences

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and resultant southerly, rain-bearing winds during the summer. The semiarid

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CHAPTER 8: Introduction to the Hydrosphere (e). Cloud Formation Processes.

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The influence of the Southwest Monsoon is felt as far north as in China's

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oceans. (The cool air then flows towards the land to complete the cycle.)

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peninsula. This is known as the Northeast Monsoon or Retreating Monsoon.

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over the land. This is why summer monsoons cause so much rain over land.

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The southwestern summer monsoons occur from June through September. The

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and the great seasonal temperature and humidity differences between the

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Strengthening of the Asian monsoon has been linked to the uplift of the

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Wang, Pinxian; Clemens, Steven; Tada, Ryuji; Murray, Richard (2019).

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The etymology of the word monsoon is not wholly certain. The English

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Chang, C.P., Wang, Z., Hendon, H., 2006, The Asian Winter Monsoon.

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during boreal winter. It is associated with the development of the

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Matsuzaki, Kenji M.; Ikeda, Masayuki; Tada, Ryuji (20 July 2022).

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This article is about the seasonal winds. For other uses, see

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Seasonal changes in atmospheric circulation and precipitation

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International Committee of the Third Workshop on Monsoons.

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10.1130/0091-7613(2003)031<0047:IONHGA>2.0.CO;2

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International Committee of the Third Workshop on Monsoons.

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Advancing monsoon clouds and showers in Aralvaimozhy, near

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depend upon this pattern for most of their precipitation.

985:(LC). The weakening of the LC would have an effect on the 747: 3305: 1876: 567: 3516: 2035:

towards the vast spans of the Indian Ocean south of the

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temperature, while land temperatures are more variable.

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Pages displaying short descriptions of redirect targets

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in Japan, with the latter two resembling frontal rain.

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The major monsoon systems of the world consist of the

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Quarterly Journal of the Royal Meteorological Society

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Indo-Australian/Borneo-Australian/Australian monsoon

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Monsoon clouds arriving at Port Blair, Andaman, India

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National Weather Service: The North American Monsoon

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