Haboob

From Wikipedia, the free encyclopedia
A haboob moves across the Llano Estacado toward Yellow House Canyon, near the residential community of Ransom Canyon, Texas (18 June 2009)
Part of a series on
Weather
Global tropical cyclone tracks-edit2.jpg
Temperate and polar seasons
Tropical seasons
Storms
Precipitation
Topics
Glossaries
Cumulus clouds in fair weather.jpeg Weather portal
  • v
  • t

A haboob (Arabic: هَبوب, romanized: habūb, lit. 'blasting/drifting') is a type of intense dust storm carried on an atmospheric gravity current, also known as a weather front. Haboobs occur regularly in dry land area regions throughout the world.

Description[]

During thunderstorm formation, winds move in a direction opposite to the storm's travel, and they move from all directions into the thunderstorm. When the storm collapses and begins to release precipitation, wind directions reverse, gusting outward from the storm and generally gusting the strongest in the direction of the storm's travel.[1][2][3]

When this downdraft of cold air, or downburst, reaches the ground, it blows dry, loose silt and clay (collectively, dust) up from the desert, creating a wall of sediment that precedes the storm cloud. This wall of dust can be up to 100 km (62 mi) wide and several kilometers in elevation. At their strongest, haboob winds often travel at 35–100 km/h (22–62 mph), and they may approach with little or no warning. Often rain does not appear at ground level as it evaporates in the hot, dry air (a phenomenon known as virga). The evaporation cools the rushing air even further and accelerates it. Occasionally, when the rain does persist, it can contain a considerable quantity of dust. Severe cases are called mud storms. Eye and respiratory system protection is advisable for anyone who must be outside during a haboob. Moving to shelter is highly advised during a strong event.

Occurrence[]

Middle East[]

Haboobs have been observed in the Sahara, Sahel (typically Sudan, where they were named and described), as well as across the Arabian Peninsula, throughout Kuwait, and in the most arid regions of Iraq.[4] Haboob winds in the Arabian Peninsula, Iraq, Kuwait are frequently created by the collapse of a thunderstorm.

North Africa[]

African haboobs result from the northward summer shift of the Intertropical Convergence Zone into North Africa, bringing moisture from the Gulf of Guinea.

Australia[]

Haboobs in Australia may be frequently associated with cold fronts. The deserts of Central Australia, especially near Alice Springs, are particularly prone to haboobs, with sand and debris reaching several kilometers into the sky and leaving up to 30 centimetres (1 ft) of sand in the haboob's path.

North America[]

See also: North American Monsoon

As with haboobs in the Middle East, haboob occurrences in North America are often created by the collapse of a thunderstorm. This is a local or mesoscale event, and at times of extreme drought they can originate in agricultural regions. Some of the most famous dust storms of the Dust Bowl and similar conditions later were in fact synoptic scale events typically generated by a strong cold frontal passage, with 14 April 1935, 9–11 May 1934, 19 February 1954, and 11 November 1911 being particularly vivid examples.

The arid and semiarid regions of North America—in fact, any dry region—may experience haboobs. In North America, the most common terms for these events are either dust storm or sandstorm. In the U.S., they frequently occur in the deserts of Arizona, including around the cities of Yuma and Phoenix;[5][6] in New Mexico, including Albuquerque; in eastern California, and in Texas.[7] They also sometimes occur in the Columbia Basin, of Eastern Washington, almost always leading to an impact with the city of Spokane. If the storms are strong enough, they can reach as far east as Post Falls and Moscow, in North Idaho.

Mars[]

Global dust storms on Mars have been compared to haboobs on Earth.[8]

Titan[]

Dust storms of Titan observed in 2009 and 2010 have been compared to haboobs.[9][10] However, the convective storm clouds are composed of liquid methane droplets, and the dust is likely composed of organic tholins.[10]

See also[]

References[]

  1. ^ Farquharson, J. S. (1937). "Haboobs and instability in the sudan". Quarterly Journal of the Royal Meteorological Society. 63 (271): 393–414. Bibcode:1937QJRMS..63..393F. doi:10.1002/qj.49706327111.
  2. ^ Lawson, T. J. (1971). "Haboob Structure at Khartoum". Weather. 26 (3): 105–112. Bibcode:1971Wthr...26..105L. doi:10.1002/j.1477-8696.1971.tb07402.x.
  3. ^ Membery, D. A. (1985). "A Gravity-Wave Haboob?". Weather. 40 (7): 214–221. Bibcode:1985Wthr...40..214M. doi:10.1002/j.1477-8696.1985.tb06877.x.
  4. ^ Sutton, L. J. (1925). "Haboobs". Quarterly Journal of the Royal Meteorological Society. 51 (213): 25–30. Bibcode:1925QJRMS..51...25S. doi:10.1002/qj.49705121305.
  5. ^ Idso, S. B.; Ingram, R. S.; Pritchard, J. M. (1972). "An American Haboob". Bulletin of the American Meteorological Society. 53 (10): 930–935. Bibcode:1972BAMS...53..930I. doi:10.1175/1520-0477(1972)053<0930:AAH>2.0.CO;2.
  6. ^ Idso, Carolyn W. (1973). "Haboobs in Arizona". Weather. 28 (4): 154–155. Bibcode:1973Wthr...28..154I. doi:10.1002/j.1477-8696.1973.tb02253.x.
  7. ^ Chen, W.; Fryrear, D. W. (2002). "Sedimentary characteristics of a haboob dust storm". Atmospheric Research. 61 (1): 75–85. Bibcode:2002AtmRe..61...75C. doi:10.1016/S0169-8095(01)00092-8.
  8. ^ Boyle, R. (2017). "Everything About Mars Is The Worst." FiveThirtyEight. Retrieved 9 March 2017, from https://fivethirtyeight.com/features/everything-about-mars-is-the-worst/
  9. ^ Keane, James Tuttle (October 2018). "Haboobs on Titan". Nature Geoscience. 11 (10): 705. Bibcode:2018NatGe..11..705K. doi:10.1038/s41561-018-0240-3. ISSN 1752-0908. S2CID 135135003.
  10. ^ a b Rodriguez, S.; Le Mouélic, S.; Barnes, J. W.; Kok, J. F.; Rafkin, S. C. R.; Lorenz, R. D.; Charnay, B.; Radebaugh, J.; Narteau, C.; Cornet, T.; Bourgeois, O. (October 2018). "Observational evidence for active dust storms on Titan at equinox". Nature Geoscience. 11 (10): 727–732. Bibcode:2018NatGe..11..727R. doi:10.1038/s41561-018-0233-2. ISSN 1752-0908. S2CID 134006536.

External links[]

Retrieved from ""