Actual wind erosion rates are determined by a combination of wind conditions and the physical condition of the soil or sediment surface. The vertical profile of wind speeds and the extent of vertical turbulence are key wind components. The directional persistence of strong winds is also a factor, especially for surface creep and saltation processes. The most important aspects related to the soil or sediment surface include:
# surface moisture conditions,
# the extent of nonerodible surface material,
# the extent of particle aggregation in the erodible material, and
# the size of the exposed area.
Wet or frozen surfaces are essentially immune to wind erosion. Chepil and Woodruff (1963) determined that surface moisture levels above the permanent wilting point (15 atmospheres suction) effectively protect soil surfaces from wind erosion. Shikula (1981) examined the effect of atmospheric moisture levels on the threshold wind speed associated with dust storm events in Ukraine. Atmospheric moisture levels were characterized as a moisture deficit (the difference between actual water vapor pressure and the saturation vapor pressure level). A strong correlation was found between threshold wind speeds for initiating dust storms and moisture deficit levels. The threshold wind speed averaged 12.1 mph at a moisture deficit of 35 millibars, 19.9 mph at a moisture deficit of 25 millibars, 27.7 mph at a moisture deficit
of 15 millibars, and 35.6 mph at a moisture deficit of 5 millibars.
The presence of nonerodible surface material (e.g., rocks, vegetation, or chemically cemented sediments) normally reduces the potential for wind erosion by reducing wind speeds near the ground and blocking surface creep and saltation movements. However, very sparse coverage by nonerodible material may sometimes induce small-scale air turbulence that enhances the erosion of fine surface sediments by suspension.
Particle aggregation in erodible material can have complicated effects. The ggregates may result in surface characteristics that raise portions of the soil or sediment above the laminar layer. The size and density of the aggregates will also affect the minimum wind velocity necessary to initiate particle movement.
Saltation, ballistic impact, and airborne collisions among aggregates often break the aggregates apart into particles small enough to be carried in suspension as opposed to saltation or surface creep.
The size and dimensions of areas susceptible to wind erosion also have some effect on wind erosion rates. These size factors are most important for surface creep and saltation processes and are less important for particle removal by suspension transport.
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Actual wind erosion rates are determined by a combination of wind conditions and the physical condition of the soil or sediment surface. The vertical profile of wind speeds and the extent of vertical turbulence are key wind components. The directional persistence of strong winds is also a factor, especially for surface creep and saltation processes. The most important aspects related to the soil or sediment surface include:
# surface moisture conditions,
# the extent of nonerodible surface material,
# the extent of particle aggregation in the erodible material, and
# the size of the exposed area.
Wet or frozen surfaces are essentially immune to wind erosion. Chepil and Woodruff (1963) determined that surface moisture levels above the permanent wilting point (15 atmospheres suction) effectively protect soil surfaces from wind erosion. Shikula (1981) examined the effect of atmospheric moisture levels on the threshold wind speed associated with dust storm events in Ukraine. Atmospheric moisture levels were characterized as a moisture deficit (the difference between actual water vapor pressure and the saturation vapor pressure level). A strong correlation was found between threshold wind speeds for initiating dust storms and moisture deficit levels. The threshold wind speed averaged 12.1 mph at a moisture deficit of 35 millibars, 19.9 mph at a moisture deficit of 25 millibars, 27.7 mph at a moisture deficit
of 15 millibars, and 35.6 mph at a moisture deficit of 5 millibars.
The presence of nonerodible surface material (e.g., rocks, vegetation, or chemically cemented sediments) normally reduces the potential for wind erosion by reducing wind speeds near the ground and blocking surface creep and saltation movements. However, very sparse coverage by nonerodible material may sometimes induce small-scale air turbulence that enhances the erosion of fine surface sediments by suspension.
Particle aggregation in erodible material can have complicated effects. The ggregates may result in surface characteristics that raise portions of the soil or sediment above the laminar layer. The size and density of the aggregates will also affect the minimum wind velocity necessary to initiate particle movement.
Saltation, ballistic impact, and airborne collisions among aggregates often break the aggregates apart into particles small enough to be carried in suspension as opposed to saltation or surface creep.
The size and dimensions of areas susceptible to wind erosion also have some effect on wind erosion rates. These size factors are most important for surface creep and saltation processes and are less important for particle removal by suspension transport.