Let us make the following variable transformation in eq. (56): equation(57) ξ=ε(m˜4)1/2.After substituting the above relation we obtain equation(58) f(ξ)=ξIuIcexp [−ξ24IuIc] I0 [ξ24Iu−IcIuIc].This probability density function will be used to examine some special cases of directional spreading. In particular, when the wave energy is uniformly distributed in all directions, the directional selleck chemicals llc spreading takes the form equation(59) D(Θ)=12π.Then the probability density function (eq. (54)) becomes equation(60) f(ε,θ1)=επm˜4exp(−ε2m˜4),and after integration against angle θ  1 we have equation(61) f(ε)=2εm˜4exp(−ε2m˜4).Therefore, for short-crested and uniformly distributed waves,

the surface slope distribution is the Rayleigh distribution, which, contrary to expectation, does not depend on the direction θ  1. The ratio of the mean square slopes σu2 and σc2 is equation(62) σc2σu2=IcIu=1. On the other hand, it can be shown that for very narrow directional spreading, when all spectral wave components propagate along the x axis, the directional spreading is simply equation(63) D(Θ)=δ(Θ−Θ0),D(Θ)=δ(Θ−Θ0),where Θ0 = 0, and the probability density function ( eq. (58)) becomes equation(64) f(ξ)=2πexp(−12ξ2).The above equation indicates that when wave crests are very long (a very narrow directional distribution), surface slopes are normally distributed (truncated normal distribution). The directional spreading function frequently used in practice has the

form as in eq. (20). For very narrow directional spreading (s   ≥ 10), the integrals in eq. (52) become Iu   → 1 and Ic   → 0. Thus, almost all the wave energy Lapatinib propagates along the wind direction, whereas the amount of energy in the cross-wind direction is very small. Therefore, Ic  /Iu   → 0. On the other hand, for small values of the directionality parameter s  , both integrals Iu   and Ic   are 5-Fluoracil almost the same, i.e. lims→0(Ic/Iu)=1, and the wave energy becomes uniformly distributed in all directions. The mean square slopes σu2 and σc2 follow from eq. (50). Therefore we have equation(65) σu2=0.076a4(gXU2)−0.22Iuσc2=0.076a4(gXU2)−0.22Ic},where coefficient a4 is given in eq. (19). The above equations indicate that the ratio of the mean square slopes

σc2/σu2 does not depend on the frequency characteristics of the wave field and is a function of the directional spreading only. Table 1 shows the ratio of the mean square slopes for selected values of the directionality parameter s. It should be noted that the observed cross-wind component of the mean square slope can be very high and for some s values even equal to the up-wind component. To define the relationship between the mean-square-slopes and the wind speed U10 and wind fetch X we again use Cox & Munk’s (1954) data. In this experiment, however, the exact values of the wind fetches are not known. Thus in Figure 2, the up-wind mean-square slope is shown for three specified wind fetches, i.e. X = 10, 50 and 100 km and directional spreading cos2 (Θ).