By Richard Soulsby


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2. The tidal current velocity profile throughout the water column is given with reasonable accuracy by (Soulsby, 1990): f o r 0 5 { < z < * ( m where U is the depth-averaged current speed, h = water depth 48 CURRENTS Table 7. 4). and 6 is the boundary-layer thickness. Equation (26a) is compatible with Equation (22) near the bed. g. g. / = 1-1914 x 10~ 4 rads" 1 at latitude 55°N) C/a and Ub = maximum and minimum values of the depthaveraged current speed through a tidal cycle. By convention, Ub is negative if the tidal current vector rotates clockwise (viewed from above) in the northern hemisphere.

The bulk velocity F B is the discharge of water per unit area of bed normal to the flow direction. It is thus a smaller velocity (by a factor e) than the velocity of the water flowing between the grains. The pressure gradient has been written as dpjdz, 37 DYNAMICS OF MARINE SANDS appropriate to a vertical flow, but Equation (9) can be adapted to apply to any direction. The hydraulic gradient is a measure of the pressure gradient in which the pressure is expressed as head of water, and hence / is dimensionless.

5. GENERAL PROCEDURE FOR SEDIMENT STUDIES The following sets out a general procedure to follow for solving a wide variety of sediment-related problems. There is, in fact, no standard or widely-accepted procedure established for such 12 INTRODUCTION problems, and the following is purely a personal approach suggested by the author. The procedure should be adapted to the specific problem, and rarely (if ever) will every step need to be taken. In some steps, rather simplified rules are given, and specific Sections should be referred to if a more detailed account is required.

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