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in describing soil, it is important to give preference to the portion of the soil surface that is most easily identified and most likely to be encountered in the field. soil surface textures have a greater significance than any differences in depth, and those differences should be described only when the soil surface is not characteristic. some of the most common site descriptions are listed here, along with illustrations of sample soil surfaces. using a map or grid as a guide, describe the character of the soil surface. for a map or grid that is not described in the land-cover and land-use literature, the following procedure is used to describe the typical soil type for that map or grid. the description must show soil depth, horizon type, parent materials, and geologic formations. the size, shape, appearance, and color of the soil surface must be well described. typical methods of describing or classifying soils are described in the text.
the client-weighing method of determining bulk density may be used for soils with particle sizes up to about 250 mm for coarse-textured soils and greater than about 80% fine-textured soils. for soils containing clay particles with sizes larger than about 250 mm, the soil sample should be piped through a 100-mesh sieve. the filtered soil sample is then mixed with a 1:1 slurry of soil and air and allowed to drain for a short period of time. the soil sample is weighed before and after the drying process to determine the dry soil weight. bulk density is calculated as the difference between the two weights divided by the original soil sample volume. standard error is the square root of the difference between the two weights. an appropriate soil sample must be used for the purpose. samples taken from areas that have a large clay content may not have a uniform clay size distribution. when used, specify which type of standard error was used.
the clay content of the soil can be determined by the wet sieving of a soil sample for the fractions passing 100 and 250-mesh sieves. the clay content percentage is calculated by dividing the weight of the clay fraction by the total soil weight.
soil aggregates do not bind together until they have been subjected to a long-term, periodical shear force in the field or during transportation. organic matter in soil may affect the physical properties of soil aggregates in a number of ways, including: rheology, bonding of individual particles, and formation and decomposition of aggregates.
the physical and chemical properties of soils and the uses of soils are described in soil and rock types for north america (usda, 1994). these properties are also described in the companion publication soils of the united states and canada (usda, 1998). acronyms used in this chapter are defined in the appendix.
downhole conditions are characterized by a complex set of factors including soil and rock type, quality of the formation water and the quality of water in place, aqueous materials, and the presence or absence of ice and sediments. the presence of ice and sediments may prevent good penetration of water into the soil. to characterize permeability, it is necessary to determine the nature and location of the ice and sediment. the presence or absence of ice and sediments generally is described by a numerical code, and the depth to the ice or sediment may be stated with some accuracy. the specific permeability of an unsaturated zone is not generally known. the infiltration rate, in general, can be calculated by dividing the rate of saturation loss or the rate of water flow by the specific conductivity of the soil. the term permeability is defined with reference to the pore space in the soil. according to the current definition, permeability is a measure of the ease with which water in the soil pore spaces passes through the soil. it does not distinguish among differing forms of water found in soils.
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