Download e-book for kindle: Computational river dynamics by Weiming Wu

By Weiming Wu

ISBN-10: 0203938488

ISBN-13: 9780203938485

ISBN-10: 041544960X

ISBN-13: 9780415449601

ISBN-10: 0415449618

ISBN-13: 9780415449618

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 combination and coupling of those versions. features a extensive choice of numerical tools for open-channel flows, similar to the SIMPLE(C) algorithms on staggered and non-staggered grids, the projection strategy, and the flow functionality and vorticity process. The state of the art in sediment delivery modeling ways is defined, equivalent to non-equilibrium delivery versions, non-uniform total-load delivery versions, and semi-coupled and paired systems for move and sediment calculations. Sediment delivery thought is mentioned and lots of newly-developed, non-uniform sediment shipping formulae are awarded. the various labored examples illustrate numerous stipulations, akin to reservoir sedimentation; channel erosion because of dam development; channel widening and meandering; neighborhood scour round in-stream hydraulic buildings; plants results on channel morphodynamic approaches; cohesive sediment shipping; dam-break fluvial strategies and contaminant shipping. steered as a reference advisor for river and hydraulic engineers and as a path textual content for instructing sediment delivery modeling, computational free-surface move, and computational river dynamics to senior scholars.

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7; Aδ is the cross-sectional area of the bed-load zone; Qb is the bed-load transport rate at the cross-section; and Cδ is the laterally-averaged bed-load concentration. In analogy to Eq. 90), by using Cδ = Qb /(Aδ Ub ), Eq. 109) can be rewritten as (1 − pm ) ∂Ab ∂ + ∂t ∂t Qb Ub + ∂Qb = B(Db − Eb ) ∂x where Ub is the laterally-averaged velocity of bed load. 110) 42 Computational River Dynamics Summing Eqs. 111) where Ct is the total-load concentration averaged over the cross-section, defined as Ct = (Qb + As U C)/(AU); and βˆt is a correction factor for total load, related to βˆs and Ub by βˆt = ACt /(AC/βˆs + Qb /Ub ) = 1/[rs /βˆs + (1 − rs )U/Ub ], which is similar to Eq.

It is often assumed that As ≈ A. Integrating Eq. 107) As Note that no dispersion term appears in Eq. 106), due to the definition of C in Eq. 105). However, if C is defined by Eq. 100), a dispersion term should appear in Eq. 106). Normally, the diffusion term in Eq. 108) Integrating Eq. 109) where ∂Ab /∂t is the rate of change in bed area; Ab is the cross-sectional area of the bed above a reference datum, as shown in Fig. 7; Aδ is the cross-sectional area of the bed-load zone; Qb is the bed-load transport rate at the cross-section; and Cδ is the laterally-averaged bed-load concentration.

3. 3 Complexity of adaptation coeff icient of sediment Effect of cross-sectional shape The value of α in the 1-D model is related to the cross-sectional shape. This is demonstrated by the following analysis suggested by Zhou and Lin (1998).

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Computational river dynamics by Weiming Wu

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