To assess wind erosion as a source of atmospheric soil particles, vertical aerosol fluxes near the ground in an eroding field were computed by assuming a vertical transport mechanism similar to that for momentum. Aerosol gradients were measured by jet impactors located 1.5 and 6 m above the ground, and wind velocity gradients were measured by totalizing-three-cup anemometers located 1.5, 3 and 6 m above the ground. Information on the aerosol size distributions and quantity in the size range 0.3 ≤ r ≤ 6 μm was obtained for a variety of erosive conditions in a field in rural Nebraska. In general, the size distributions in this range suggest the power law, dN/d(log r) ∝r−2 for 1 ≤ r ≤ 6 μm, and a flatter curve for 0.3 ≤ r ≤ 6 μm. The relation of the aerosol size distribution in the range 0.3 ≤ r ≤ 6 μm to the size distribution of soil was determined. Averaged soil size distributions characteristic of the sampling field, the area within a six-mile radius of the sampling field, and soil flowing (creep... Abstract To assess wind erosion as a source of atmospheric soil particles, vertical aerosol fluxes near the ground in an eroding field were computed by assuming a vertical transport mechanism similar to that for momentum. Aerosol gradients were measured by jet impactors located 1.5 and 6 m above the ground, and wind velocity gradients were measured by totalizing-three-cup anemometers located 1.5, 3 and 6 m above the ground. Information on the aerosol size distributions and quantity in the size range 0.3 ≤ r ≤ 6 μm was obtained for a variety of erosive conditions in a field in rural Nebraska. In general, the size distributions in this range suggest the power law, dN/d(log r) ∝r−2 for 1 ≤ r ≤ 6 μm, and a flatter curve for 0.3 ≤ r ≤ 6 μm. The relation of the aerosol size distribution in the range 0.3 ≤ r ≤ 6 μm to the size distribution of soil was determined. Averaged soil size distributions characteristic of the sampling field, the area within a six-mile radius of the sampling field, and soil flowing (creep...