Chapter Overview

Learning Objectives

1. Deserts receive less than 25 cm of rainfall (or snowfall) a year, but can have either hot or cold climate. Most deserts are associated with falling, dry air masses concentrated in a belt 10 degree - 15 degree wide centered on 30 degrees north and south latitude and at the poles. Other controls include rain shadow effects, great distance from the ocean, and proximity to cold ocean currents. Deserts typically lack through-flowing streams and have internal drainage that may develop local base levels.

2. Running water is the dominant agent of landscape development in deserts because of limited vegetation. Thunderstorms commonly cause flash floods and mudflows in deserts, although stream valleys, called arroyos, are usually dry.

3. Resistance of rocks is controlled by climate and rocks that might be weathered quickly in other environments (e.g. limestone) are resistant in desert settings. Soils are coarse and rocky, and creep is common.

4. Resistant rocks in desert settings form flat-topped plateaus, mesas, and buttes depending on their size, although those features can be found in humid climates as well. Dipping beds form hogbacks and cuestas. In contrast to humid regions, desert landscapes are typically angular, although shales form gentle slopes of badland topography.

5. Internal drainages in desert settings develop playa lakes, that dry into playas, covered with either mud or salt. Coalescing alluvial fans form bajadas near the bases of mountains. Erosion of mountains produces sloping surfaces covered by a veneer of gravel called pediments that may pass into bajadas.

6. Wind is responsible for erosion of fine sediment in deserts. Like water, the faster the wind blows, the more sediment it can move, but its density limits erosion to only the finer sediment sizes. Once eroded by deflation, silt and clay can remain suspended for long periods and can be carried great distances (Saharan sediment reaches the West Indies). Sand, in contrast, moves by saltation near to the ground. Sandblasting forms ventifacts and sculpts bedrock exposures. Blowouts are depressions caused by wind erosion (deflation).

7. Wind deposited silt and clay is called loess and it is usually associated with deflation of outwash plains formed during the Pleistocene throughout the northern hemisphere.

8. Sand dunes are mounds of loose sand deposited by wind. The sand grains can be of any composition, but are typically well sorted and well rounded. The dunes are asymmetric, steep on their downwind side and gentle on their upwind side. The downwind side or slip face is steep because the slope is at the angle of repose for dry sand (34 degrees). Slip faces form the cross-bedding preserved in dune sandstones. Movement of the dune is in the direction of the slip face, because of erosion on the upwind side and transportation along the dune surface.

9. Dune geometry is controlled by wind velocity, direction, sand supply, and vegetation cover. Large dune fields are sand seas. Many dunes are irregular, but some patterns may be recognized. Low sand supply is characterized by barchan dunes, with horns pointing downwind. High sand areas may form transverse or longitudinal dunes that are elongate, or parabolic dunes around blowouts, with horns pointing upwind.

Related Readings

Bagnold, R. A. 1941. The Physics of Blown Sand and Desert Dunes. New York: William Morrow, 1954 (reprinted).

Blackwelder, E. 1954. Geomorphic Processes in the Desert. Bulletin of California Division of Mines 170:11-20. Sacramento: Department of Natural Resources.

Brookfield, M. E., and T. S. Ahlbrandt. 1983. Eolian Sediments and Processes. New York: Elsevier.

Cooke, R. U., and A. Warren. 1973. Geomorphology in Deserts. Berkeley: University of California Press.

Easterbrook, D. J. 1993. Surface Processes and Landforms. New York: Macmillan.

Glennie, K. W. 1970. Desert Sedimentary Environments. New York: Elsevier.

Greeley, R., and J. Iverson. 1985. Wind as a Geological Process. Cambridge: Cambridge University Press.

Mabbutt, J. A. 1977. Desert Landforms. Cambridge, MA: MIT Press.

McGinnies, W. G., B. J. Goldman, and P. Paylore, eds. 1968. Deserts of the World. Tucson, AZ: University of Arizona Press.

McKee, E. D., ed. 1979. A Study of Global Sand Seas. U.S. Geological Survey Professional Paper 1052.

Pewe, T. L., ed. 1981. Desert Dust: Origin, Characteristics, and Effect on Man. Boulder, CO: Geological Society of America Special Paper 186.

Pye, K., and H. Tsoar. 1990. Aeolian Sand and Sand Dunes. New York: Harper Collins Academic.

Ritter, D. F., R. C. Kochel, and J. R. Miller. 1995. Process Geomorphology. 3d ed. Dubuque, IA: Wm. C. Brown Publishers.

Sheridan, D. 1981. Desertification of the United States. Washington, D.C.: Council on Environmental Quality.

Walker, A. S. 1982. Deserts of China. American Scientist 70(4): 366-76.

Wells, S. G., and D. R. Haragan, eds. 1983. Origin and Evolution of Deserts. Albuquerque: University of New Mexico Press.

Answers to EOC Questions

Following are answers to the End of Chapter Questions for Chapter 13:

Boxed Readings