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A writer and a photographer explore the legacy of human enterprise and the wind in the California desert. Learn about the different types of winds, their effects and their meanings in this essay and photo gallery.
Desert Winds offers Independent, Assisted and Memory Care in Peoria, AZ. Enjoy spacious apartments, resort style dining, stunning courtyard views and 24-hour onsite staff.
- Overview
- Winds
- Formation and growth of dunes
Winds have three sources of variation that are important—namely, direction, velocity, and turbulence. Most of the great deserts are found in the subtropical areas of high atmospheric pressure, where the winds circulate in a clockwise direction in the Northern Hemisphere and a counterclockwise direction in the Southern Hemisphere. The high-pressure systems tend to dip down to the east so that winds are stronger there, a pattern mirrored by the dunes. Poleward of these circulation systems are the zones of eastward moving depressions in which there are generally westerly winds that mold the dunes of the North American and Central Asian deserts and of the northern Sahara. The boundaries between these two circulation systems migrate back and forth seasonally, so that complicated dune patterns are found in the zones of overlap. Only a few deserts, notably the Thar Desert of India and the Sonoran Desert of the American Southwest, are affected by monsoonal wind systems. Some dunes are built by sea breezes and local winds, as in coastal Peru.
The direction of the wind at any one place in the desert is affected by a number of local factors. Winds are particularly channeled around topographical features, such as the Tibesti Massif in the Sahara, so that dunes are affected by different winds on different sides of the obstruction. Winds also can be channeled around the dunes themselves, thereby developing patterns of secondary flow that modify the shapes of the dunes.
The pattern of wind velocity also is important. Like many natural phenomena, wind velocities have a log-normal distribution: there are a large number of moderate breezes and a diminishing number of increasingly more violent winds. The greatest volumes of sand are probably moved by unusually strong winds, because the amount of sand moved by wind is a power function (exponential factor) of the wind speed. For example, a 10-km-per-hour wind carries 13 grams per hour (0.39 ounce per hour), a 20-km-per-hour wind carries 274 grams per hour, and a 30-km-per-hour wind carries 1,179 grams per hour. A wind of a particular velocity will move fewer larger than smaller grains. Strong winds often blow from a particular direction, as in the southern Sahara, where the intense winds of sandstorms come predominantly from one direction. Such winds are responsible for the undulations of the sand sheets, because they alone can move coarse sands. Lighter winds blow from several different directions, and the dunes, being of finer sand, are therefore affected by several winds.
The wind is retarded near the surface by friction. Above the ground the wind velocity increases rapidly. The near-surface velocity must rise above a certain threshold value before sand will be picked up, the value depending on the size of the sand grains; for example, a wind of 12 km per hour measured at a height of 10 metres is required to move sands 0.02 centimetre in diameter, and a 21-km-per-hour wind is required to move 0.06-cm sands. Once sand movement has been initiated by wind of such velocity, it can be maintained by winds blowing at lower speeds. Because instantaneous wind speeds in eddies can rise well above the average velocity, turbulence also is important, but it is difficult to measure.
Winds have three sources of variation that are important—namely, direction, velocity, and turbulence. Most of the great deserts are found in the subtropical areas of high atmospheric pressure, where the winds circulate in a clockwise direction in the Northern Hemisphere and a counterclockwise direction in the Southern Hemisphere. The high-pressure systems tend to dip down to the east so that winds are stronger there, a pattern mirrored by the dunes. Poleward of these circulation systems are the zones of eastward moving depressions in which there are generally westerly winds that mold the dunes of the North American and Central Asian deserts and of the northern Sahara. The boundaries between these two circulation systems migrate back and forth seasonally, so that complicated dune patterns are found in the zones of overlap. Only a few deserts, notably the Thar Desert of India and the Sonoran Desert of the American Southwest, are affected by monsoonal wind systems. Some dunes are built by sea breezes and local winds, as in coastal Peru.
The direction of the wind at any one place in the desert is affected by a number of local factors. Winds are particularly channeled around topographical features, such as the Tibesti Massif in the Sahara, so that dunes are affected by different winds on different sides of the obstruction. Winds also can be channeled around the dunes themselves, thereby developing patterns of secondary flow that modify the shapes of the dunes.
The pattern of wind velocity also is important. Like many natural phenomena, wind velocities have a log-normal distribution: there are a large number of moderate breezes and a diminishing number of increasingly more violent winds. The greatest volumes of sand are probably moved by unusually strong winds, because the amount of sand moved by wind is a power function (exponential factor) of the wind speed. For example, a 10-km-per-hour wind carries 13 grams per hour (0.39 ounce per hour), a 20-km-per-hour wind carries 274 grams per hour, and a 30-km-per-hour wind carries 1,179 grams per hour. A wind of a particular velocity will move fewer larger than smaller grains. Strong winds often blow from a particular direction, as in the southern Sahara, where the intense winds of sandstorms come predominantly from one direction. Such winds are responsible for the undulations of the sand sheets, because they alone can move coarse sands. Lighter winds blow from several different directions, and the dunes, being of finer sand, are therefore affected by several winds.
The wind is retarded near the surface by friction. Above the ground the wind velocity increases rapidly. The near-surface velocity must rise above a certain threshold value before sand will be picked up, the value depending on the size of the sand grains; for example, a wind of 12 km per hour measured at a height of 10 metres is required to move sands 0.02 centimetre in diameter, and a 21-km-per-hour wind is required to move 0.06-cm sands. Once sand movement has been initiated by wind of such velocity, it can be maintained by winds blowing at lower speeds. Because instantaneous wind speeds in eddies can rise well above the average velocity, turbulence also is important, but it is difficult to measure.
The dune-forming process is complex, particularly where many thousands of dunes have grown side-by-side in sand seas. Yet, an introductory account can be given based on the example of a single dune on a hard desert surface.
Most of the sand carried by the wind moves as a mass of jumping (saltating) grains; coarser particles move slowly along the surface as creep and are kept in motion partly by the bombardment of the saltating grains. Saltating sand bounces more easily off hard surfaces than off soft ones, with the result that more sand can be moved over a pebbly desert surface than over a smooth or soft one. Slight hollows or smoother patches reduce the amount of sand that the wind can carry, and a small sand patch will be initiated. If it is large enough, this patch will attract more sand.
The wind adjusts its velocity gradient on reaching the sand patch; winds above a certain speed decrease their near-surface velocity and deposit sand on the patch. This adjustment takes place over several metres, the sand being deposited over this distance, and a dune is built up. The growth of this dune cannot continue indefinitely. The windward slope is eventually adjusted, so that there is an increase in the near-surface velocity up its face to compensate for the drag imposed by the sandy surface. When this happens, the dune stops growing and there is no net gain or loss of sand.
As the dune grows, the smooth leeward slope steepens until the wind cannot be deflected down sharply enough to follow it. The wind then separates from the surface leaving a “dead zone” in the lee into which falls the sand brought up the windward slope. When this depositional slope is steepened to the angle of repose of dry sand (about 32°), this angle is maintained and the added sand slips down the slope or slip face. When this happens, the dune form is in equilibrium, and the dune moves forward as a whole, sand being eroded from the windward side and deposited on the lee.
Apr 29, 2021 · How do daily temperature and wind changes in deserts affect the transport of sand and dust? A study at White Sands Dune Field reveals a daily cycle of heat and wind that influences the surface and atmosphere. Learn how this process may help improve climate models and forecast dust storms on Mars.
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Apr 19, 2021 · Climate change and ocean warming may reduce the annual dust plumes from the Sahara Desert, the largest and hottest desert in Africa, according to NASA scientists. The dust transport affects the ocean, vegetation, air quality, and storm formation across the Atlantic.
