Horton (HO) |
Horton (1940)Horton, R. E. (1940). An approach toward a physical interpretation of infiltration-capacity. Soil Science Society of America Journal, 5(C), 399-417. http://dx.doi.org/10.2136/sssaj1941.036159950005000C0075x. http://dx.doi.org/10.2136/sssaj1941.0361...
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f is the infiltration rate (mm/h); f0 (mm/h) and fc (mm/h) are the initial and final infiltration rates, respectively; t (h) is the time; and γ (min-1) is an empirical constant that reflects how the decay in the infiltration rates depends on the soil type and land use and management practices. |
Philip (PH) |
Philip (1957)Philip, J. R. (1957). The theory of infiltration: 1. The infiltration equation and its solution. Soil Science, 83(5), 345-358. http://dx.doi.org/10.1097/00010694-195705000-00002. http://dx.doi.org/10.1097/00010694-19570...
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Sp (mm/h-1/2) is the sorptivity, which is a function of the suction potential, and K (mm/h)is a parameter with dimension of the saturated hydraulic conductivity and is related to infiltration gravity factor. |
Green and Ampt/Mein and Larson (GA) |
Green & Ampt (1911)Green, W. H., & Ampt, G. (1911). Studies on soil physics, 1. The flow of air and water through soils. Journal of Agricultural Science, 4, 1-24. http://dx.doi.org/10.1017/S0021859600001441. http://dx.doi.org/10.1017/S0021859600001...
; Mein & Larson (1973)Mein, R., & Larson, C. (1973). Modelling infiltration during a steady rain. Water Resources Research, 9(2), 384-394. http://dx.doi.org/10.1029/WR009i002p00384. http://dx.doi.org/10.1029/WR009i002p0038...
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Kfs (mm/h) is the hydraulic conductivity of the transmission zone, which may be associated with the saturated hydraulic conductivity; hce (mm) is the effective capillarity at the wetting front; F (mm) is the cumulative infiltration at time t; and Δθ is the difference between the saturated volumetric water content (θs) and the initial volumetric water content (θi). |
Kostiakov (KV) |
Kostiakov (1932)Kostiakov, A. N. (1932). On the dynamics of the coefficient of water-percolation in soils and on the necessity for studying it from a dynamic point of view for purposes of amelioration. Soviet Soil Science, 14, 17-21.
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α (>0) and β (0<β≤1) are empirical constants related to the soil suction and hydraulic conductivity characteristics. |
Modified Kostiakov (MK) |
Mezencev (1948)Mezencev, V. J. (1948). Theory of formation of the surface runoff. Meteorologia i Gidrologia, 3, 33-40.
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α1 and β1 are empirical constants related to the suction and hydraulic conductivity characteristics. |
Holtan (HO) |
Holtan (1961)Holtan, H. N. (1961). A concept for infiltration estimates in watershed engineering (Bulletin, No. 41-51). Washington: Agricultural Research Service, U.S. Department of Agriculture
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a and n are constants that characterize how the soil type and surface layer conditions depend on the type of land use and management practices; So (mm) is the initial potential water storage in the soil, which is represented by the water deficit (total porosity (TP) minusinitial moisture) multiplied by a predefined depth of a permeable soil layer; and the quantity (So - F) represents the soil's capacity to store water. |
Modified Holtan (MH) |
Huggins & Monke (1966)Huggins, L. F., & Monke, E. J. (1966). The mathematical simulation of the hydrology of small watersheds (Technical Report, No. 1, 130 p.). Indiana: Resources Research Center, Purdue University Water.
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a1 and n1 are constants that depend on the type of soil and the type of land use and management practices, respectively. |
Singh & Yu (SY) |
Singh & Yu (1990)Singh, V. P., & Yu, F. X. (1990). Derivation of infiltration equation using systems approach. Journal of Irrigation and Drainage Engineering, 116(6), 837-858. http://dx.doi.org/10.1061/(ASCE)0733-9437(1990)116:6(837). http://dx.doi.org/10.1061/(ASCE)0733-943...
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where A, m and y are constants that depend on the characteristics of the infiltration conditions, which are obtained by fitting experimental data, and S(t) is the water storage available at time t. |