where Hu is the depth to the local subsurface saturated layer, du equals soil depth d if (Hu − d) > ψae; otherwise, du = (Hu − ψae) (i.e., integrate from 0 to d if the depth to soil water content at ψae is below d; otherwise, integrate to depth of soil water content at ψae). Since we know the running average soil moisture content in the soil θ, Equation (C2) is solved for Hu to obtain the depth to saturation of the hydrostatic equilibrium profile corresponding to θ. The estimated depth to saturation
is used to calculate the average soil moisture of the top 10 soil centimeters of the hydrostatic soil moisture profile,
Also four other corrections should be noted:
Maneta, M. P., and N. L. Silverman, 2013: A spatially distributed model to simulate water, energy, and vegetation dynamics using information from regional climate models. Earth Interact.,17,doi:10.1175/2012EI000472.1.