By J. P. O'Kane
This Festschrift containing 16 invited essays and papers is a tribute to the prestigious Irish hydrologist James Dooge at the party of his seventieth birthday. His former scholars, colleagues and buddies in fourteen nations, have supplied a diverse choice on his favorite issues: circulation in open channels and unsaturated soil, and in addition from his significant curiosity of modern years, huge scale hydrology and international change.
The e-book has 3 sections. the 1st part on hydrological techniques includes six papers. the second one part on huge scale hydrology has 4 papers. Six historic, reflective and philosophical essays at the earlier and way forward for the hydrological sciences shape the 3rd part of the e-book
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Additional info for Advances in Theoretical Hydrology. A Tribute to James Dooge
T h e p a r a m e t e r k may be found using field measurements of z B( r ) or simple models of saturated flow to drains. A more detailed treatment requires a two-dimensional theory of saturated/unsaturated flow. 2. Surface boundary condition for infiltration of rain 3 2 of 1 rain into peat is a prescribed flux at ζ = 0 , T h e boundary condition for infiltration equal to the rainfall rate Q ( m m ~ s " ) : fx = = /M2 θ < 0 S at ζ = 0 (18) Vapour flux is not normally considered during infiltration.
For favourable comments on its application and on t h e limitations of t h e parametric relationships used, see Scotter et al. (1988). Vauclin et al. (1979) provide a comparative survey of other numerical techniques for solving Richards' equation. The results in Figures 1 and 2 were calculated using this scheme. 3. 99. T h e reason is that the p e a t - w a t e r diffusivity function D = kl ) - ύφη/άθ decreases through several orders of magnitude as relative C = k(}l)m humidity declines from 1 by as little as 1%.
An example is shown in Figure 2 to demonstrate the use of the last solution. In the initial stage of a rainstorm, infiltration is at the potential rate, and the surface soil moisture content increases rapidly. W h e n the surface soil is saturated, the infiltration becomes soil controlled with a decreasing rate. After the rainstorm, evaporation takes place at the potential rate, and the surface soil moisture content decreases d u e to both uptake of soil moisture by evaporation and drainage by gravity.