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Monsoon trough


Monsoon trough

August position of the ITCZ and monsoon trough in the Pacific Ocean, depicted by area of convergent streamlines in the northern Pacific

The monsoon trough is a portion of the Intertropical Convergence Zone [1][2] as depicted by a line on a weather map showing the locations of minimum sea level pressure,[1] and as such, is a convergence zone between the wind patterns of the southern and northern hemispheres.

Westerly monsoon winds lie in its equatorward portion while easterly trade winds exist poleward of the trough.[3] Right along its axis, heavy rains can be found which usher in the peak of a location's respective rainy season. As it passes poleward of a location, hot and dry conditions develop. The monsoon trough plays a role in creating many of the world's rainforests.

The term "monsoon trough" is most commonly used in monsoonal regions of the Western Pacific such as Asia and Australia. The migration of the ITCZ/monsoon trough into a landmass heralds the beginning of the annual rainy season during summer months. Depressions and tropical cyclones often form in the vicinity of the monsoon trough, with each capable of producing a year's worth of rainfall in a relatively short time frame.


  • Movement and strength 1
    • Effect of wind surges 1.1
    • Embedded depressions 1.2
  • Roles 2
    • In rainy season 2.1
    • In tropical cyclogenesis 2.2
  • References 3

Movement and strength

February position of the ITCZ and monsoon trough in the Pacific Ocean, depicted by area of convergent streamlines offshore Australia and in the equatorial eastern Pacific

Monsoon troughing in the western Pacific reaches its zenith in latitude during the late summer when the wintertime surface ridge in the opposite hemisphere is the strongest. It can reach as far as the 40th parallel in East Asia during August and the 20th parallel in Australia during February. Its poleward progression is accelerated by the onset of the summer monsoon which is characterized by the development of lower air pressure over the warmest part of the various continents.[4][5][6] In the southern hemisphere, the monsoon trough associated with the Australian monsoon reaches its most southerly latitude in February,[7] oriented along a west-northwest/east-southeast axis.

Effect of wind surges

Increases in the relative vorticity, or spin, with the monsoon trough are normally a product of increased wind convergence within the convergence zone of the monsoon trough. Wind surges can lead to this increase in convergence. A strengthening or equatorward movement in the subtropical ridge can cause a strengthening of a monsoon trough as a wind surge moves towards the location of the monsoon trough. As fronts move through the subtropics and tropics of one hemisphere during their winter, normally as shear lines when their temperature gradient becomes minimal, wind surges can cross the equator in oceanic regions and enhance a monsoon trough in the other hemisphere's summer.[8] A key way of detecting whether a wind surge has reached a monsoon trough is the formation of a burst of thunderstorms within the monsoon trough.[9]

Embedded depressions

Monsoon Depression near Bangladesh

If a circulation forms within the monsoon trough, it is able to compete with the neighboring thermal low over the continent, and a wind surge will occur at its periphery. Such a circulation which is broad in nature within a monsoon trough is known as a monsoon depression. In northern hemisphere, monsoon depressions are generally asymmetric, and tend to have their strongest winds on their eastern periphery.[9] Light and variable winds cover a large area near their center, while bands of showers and thunderstorms develop within their area of circulation.[10]

The presence of an upper level jet stream poleward and west of the system can enhance its development by leading to increased diverging air aloft over the monsoon depression, which leads to a corresponding drop in surface pressure.[11] Even though these systems can develop over land, the outer portions of monsoon depressions are similar to tropical cyclones.[12] In India, for example, 6 to 7 monsoon depressions move across the country yearly,[4] and their numbers within the Bay of Bengal increase during July and August of El Niño events.[13] Monsoon depressions are efficient rainfall producers, and can cause a year's worth of rainfall when they move through drier areas such as the outback of Australia.[14]


In rainy season

View of central Kolkata after a monsoon rain.

Since the monsoon trough is an area of convergence in the wind pattern, and an elongated area of low pressure at the surface, the trough focuses low level moisture and is defined by one or more elongated bands of thunderstorms when viewing satellite imagery. Its abrupt movement to the north between May and June is coincident with the beginning of the monsoon regime and rainy seasons across South and East Asia. This convergence zone has been linked to prolonged heavy rain events in the Yangtze river as well as northern China.[2] Its presence has also been linked to the peak of the rainy season in locations within Australia.[15] As it progresses poleward of a particular location, clear, hot, and dry conditions develop as winds become westerly.[16] Many of the world's rainforests are associated with these climatological low pressure systems.[17]

In tropical cyclogenesis

Months of peak tropical cyclone activity worldwide

A monsoon trough is a significant genesis region for tropical cyclones. Vorticity-rich low level environments, with significant low level spin, lead to a better than average chance of tropical cyclone formation due to their inherent rotation. This is because a pre-existing near-surface disturbance with sufficient spin and convergence is one of the six requirements for tropical cyclogenesis.[18] There appears to be a 15-25 day cycle in thunderstorm activity associated with the monsoon trough, which is roughly half the wavelength of the Madden-Julian Oscillation, or MJO.[19] This mirrors tropical cyclone genesis near these features, as genesis clusters in 2–3 weeks of activity followed by 2–3 weeks of inactivity. Tropical cyclones can form in outbreaks around these features under special circumstances, tending to follow the next cyclone to its poleward and west.[20]

Whenever the monsoon trough on the eastern side of the summertime Asian monsoon is in its normal orientation (oriented east-southeast to west-northwest), tropical cyclones along its periphery will move with a westward motion. If it is reverse oriented, or oriented southwest to northeast, tropical cyclones will move more poleward. Tropical cyclone tracks with S shapes tend to be associated with reverse-oriented monsoon troughs.[21] The South Pacific convergence zone and South American convergence zones are generally reverse oriented.[7] The failure of the monsoon trough, or ITCZ, to move south of the equator in the eastern Pacific ocean and Atlantic ocean during the southern hemisphere summer is considered one of the reasons that tropical cyclones normally do not form in those regions.[9] It has also been noted that when the monsoon trough lies near 20 degrees north latitude in the Pacific, the frequency of tropical cyclones is 2 to 3 times greater than when it lies closer to 10 degrees north.[2]


  1. ^ a b "Monsoon trough". Glossary of Meteorology.  
  2. ^ a b c Bin Wang. The Asian Monsoon. Retrieved on 2008-05-03.
  3. ^ World Meteorological Organization. Severe Weather Information Centre. Retrieved on 2008-05-03.
  4. ^ a b National Centre for Medium Range Forecasting. Chapter-II Monsoon-2004: Onset, Advancement and Circulation Features. Retrieved on 2008-05-03.
  5. ^ Australian Broadcasting Corporation. Monsoon. Retrieved on 2008-05-03.
  6. ^ Dr. Alex DeCaria. Lesson 4 – Seasonal-mean Wind Fields. Retrieved on 2008-05-03.
  7. ^ a b U. S. Navy. 1.2 Pacific Ocean Surface Streamline Pattern. Retrieved on 2006-11-26.
  8. ^ Chih-Lyeu Chen. Effects of the Northeast Monsoon on the Equatorial Westerlies Over Indonesia. Retrieved on 2008-05-03.
  9. ^ a b c U. S. Navy. SECTION 3. DYNAMIC CONTRIBUTORS TO TROPICAL CYCLONE FORMATION. Retrieved on 2006-11-26.
  10. ^ Chip Guard. Climate Variability on CNMI. Retrieved on 2008-05-03.
  11. ^ Sixiong Zhao and Graham A. Mills. A Study of a Monsoon Depression Bringing Record Rainfall over Australia. Part II: Synoptic–Diagnostic Description. Retrieved on 2008-05-03.
  12. ^ N.E. Davidson and G.J. Holland. A Diagnostic Analysis of Two Intense Monsoon Depressions over Australia. Retrieved on 2008-05-03.
  13. ^ O. P. Singh, Tariq Masood Ali Khan, and Md. Sazedur Rahman. Impact of Southern Oscillation on the Frequency of Monsoon Depressions in the Bay of Bengal. Retrieved on 2008-05-03.
  14. ^ Bureau of Meteorology. TWP-ICE Synoptic Overview, 1 February 2006. Retrieved on 2008-05-03.
  15. ^ Bureau of Meteorology. Climate of Giles. Retrieved on 2008-05-03.
  16. ^ School of Ocean and Earth Science and Technology at the University of Hawai'i. Pacific ENSO Update: 4th Quarter 2001 - Vol. 7 No. 4. Retrieved on 2008-05-03.
  17. ^ Hobgood (2008). Global Pattern of Surface Pressure and Wind. Ohio State University. Retrieved on 2009-03-08.
  18. ^ Christopher Landsea. Climate Variability of Tropical Cyclones: Past, Present and Future. Retrieved on 2006-11-26.
  19. ^ Patrick A. Harr. Tropical Cyclone Formation/Structure/Motion Studies. Retrieved on 2006-11-26.
  20. ^ Joint Typhoon Warning Center. Typhoon Polly. Retrieved on 2006-11-26.
  21. ^ Mark A. Lander. Specific Tropical Cyclone Track Types and Unusual Tropical Cyclone Motions Associated with a Reverse-Oriented Monsoon Trough in the Western North Pacific. Retrieved on 2006-11-26.
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