Download Computational river dynamics by Weiming Wu PDF

By Weiming Wu

Comprehensive textual content at the basics of modeling movement and sediment shipping in rivers treating either actual ideas and numerical equipment for numerous levels of complexity. comprises 1-D, 2-D (both intensity- and width-averaged) and 3-D versions, in addition to the mixing and coupling of those types. incorporates a extensive choice of numerical equipment for open-channel flows, similar to the SIMPLE(C) algorithms on staggered and non-staggered grids, the projection technique, and the circulation functionality and vorticity technique. The cutting-edge in sediment delivery modeling ways is defined, akin to non-equilibrium delivery types, non-uniform total-load shipping versions, and semi-coupled and paired tactics for circulate and sediment calculations. Sediment delivery thought is mentioned and plenty of newly-developed, non-uniform sediment delivery formulae are awarded. the numerous labored examples illustrate quite a few stipulations, equivalent to reservoir sedimentation; channel erosion as a result of dam development; channel widening and meandering; neighborhood scour round in-stream hydraulic constructions; plants results on channel morphodynamic procedures; cohesive sediment shipping; dam-break fluvial methods and contaminant shipping. prompt as a reference consultant for river and hydraulic engineers and as a direction textual content for instructing sediment shipping modeling, computational free-surface move, and computational river dynamics to senior scholars.

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And τzz are the stresses (including both molecular and turbulent effects); and Fx , Fy , and Fz are the components of the resultant external force in the x-, y- and z-directions. As gravity is assumed to be the only external force, Fx = Fy = 0 and Fz = −ρg. Note that the bar “-”, denoting time-averaged quantities, is omitted in Eqs. 63) for simplicity. 64) Under the assumption of constant ρ along the depth, Eq. 6 Configuration of flow and sediment transport. 65) where zs is the water surface elevation, and pa is the atmospheric pressure at the water surface.

This concept assumes that, in analogy to the viscous stresses in Eq. 45) where νt is the turbulent or eddy viscosity; and k is the turbulent kinetic energy, defined as k = ui ui /2. In contrast to the molecular viscosity ν, the eddy viscosity νt is not a Mathematical description of flow and sediment transport 25 fluid property but strongly depends on the state of turbulence, perhaps varying largely in time and space. In most flow regions, the eddy viscosity is much larger than the molecular viscosity; thus, the latter usually is negligible.

The cumulative size frequency curve shows the percent of material finer than a given sediment size in the total sample, as shown in Fig. 1(b). For a sediment mixture with a normal size distribution, the cumulative size frequency curve is a straight line on the normal probability paper. Characteristic diameters The median diameter, d50 , is the particle size at which 50% by weight of the sample is finer. Likewise, d10 and d90 are the particle sizes at which 10% and 90% by weight of the sample are finer, respectively.

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