In addition to the pore pressure, the filtration rates in soil pores are also interesting. The components of the groundwater flow velocity vector

(u, v) satisfy the following system of equations ( Moshagen & Torum 1975): equation(4) ∂u∂t+u∂u∂x+v∂u∂z=−1nρ∂p∂x−gnKfu,∂v∂t+u∂v∂x+v∂v∂z=−1nρ∂p∂z−gnKfv,uρw∂ρ∂x+vρw∂ρ∂z+∂u∂x+∂v∂z=−nnKf∂p∂t. In the stationary case and after ignoring the non-linear members, components of the velocity vector may be determined from the measurements of pressure with formulas LY294002 resulting from Darcy’s law: equation(5) uxzt=−Kfρwg∂p∂x,vxzt=−Kfρwg∂p∂z. From relations (2) and (5), we obtain the following components of the velocity of circulation of ground water caused by a surface wave of height H and frequency ω: equation(6) uxzt=ℜiKfnkH2coshψz+hncoshkhcoshψhn−hexpikx−ωt and equation(7) vxzt=ℜKfnψH2sinhψz+hncoshkhcoshψhn−hexpikx−ωt. The wave number k

satisfies the classical dispersion relation: Compound C concentration equation(8) ω2=ghtanh(kh).ω2=ghtanhkh. Let us assume that waves move towards the shore above the bottom of a slope β. The water depth thus satisfies the following relationship: equation(9) h(x)=h1−βx,hx=h1−βx, where h1 is the initial water depth ( Figure 1). During its transformation on a sloping bottom, a wave changes its parameters: it becomes steeper and at some point in the coastal zone (point Obr) the wave breaks. The dynamics before and after the breaking point is different. Therefore, the pressure at the bottom and also the pore water pressure and pore water velocity will depend on the location in relation to the breaking point. In particular, we should distinguish two zones: the pore pressure in front of the breaking zone and behind the breaking zone (Massel et al. 2004). Experiments

on the wave channel in Hannover showed that the pore pressure in front of the breaking zone corresponds directly to the oscillation of the sea surface ζ  (x, t  ). Behind Janus kinase (JAK) the breaking zone the pore pressure changes in a different way. In addition to oscillations similar to those of the free sea surface, there is a fixed component of the hydrostatic pressure associated with the elevation of mean sea level ζ¯. Let us consider separately the two types of pore pressure and the circulation related to them. If we assume that the slope of the bottom in front of the breaking zone is very smooth, which is usually the case on sandy shores, then we can use the solution from equation (1) to determine pore pressure and circulation. The sea depth at the point where the pore pressure is aanalysed is assumed to be locally constant. The wave height at this point is calculated on the basis of H1 at the initial depth h1, or the data from observations are used.