The governing equations of stationary groundwater flow are [28]
\boldsymbol{ v} = - \boldsymbol{k} \cdot \nabla h | (360) |
(also called Darcy's law) and
\nabla \cdot \boldsymbol{ v} = 0, | (361) |
where \boldsymbol{v} is the discharge velocity, \boldsymbol{k} is the permeability tensor and h is the total head defined by
In the latter equation p is the groundwater pressure, \rho is its density and z is the height with respect to a reference level. The discharge velocity is the quantity of fluid that flows through a unit of total area of the porous medium in a unit of time.
The resulting equation now reads
\nabla \cdot (- \boldsymbol{ k} \cdot \nabla h) = 0. | (363) |
Accordingly, by comparison with the heat equation, the correspondence in Table () arises. Notice that the groundwater flow equation is a steady state equation, and there is no equivalent to the heat capacity term.
Possible boundary conditions are:
h = \frac{p_0 - \rho g z}{\rho g} + z = \frac{p_0}{\rho g}. | (364) |
h = \frac{p_0}{\rho g} + z. | (365) |
h = \frac{p_0}{\rho g} + z. | (366) |
In the direction \boldsymbol{n} perpendicular to the free surface v_n = 0 must be satisfied. However, the problem is that the exact location of the free surface is not known. It has to be determined iteratively until both equations are satisfied.