Turbulent wave boundary layers: 2. Second‐order theory and mass transport

Trowbridge, John; Madsen, Ole Secher

doi:10.1029/jc089ic05p07999

Cited by 131 publications

(114 citation statements)

References 13 publications

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“…Moreover, the present predictions are closer to the experimental data than those obtained by previous researchers (e.g. Trowbridge & Madsen 1984b). The significant differences which appear far from the bottom might be due to the finite length of the wave channel used in the experiments and the consequent offshore steady current which is present outside the boundary layer.…”

Section: The Numerical Solutioncontrasting

confidence: 52%

Sediment Transport at the Bottom of Sea Waves

Vittori

Blondeaux

2012

Int. Conf. Coastal. Eng.

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The flow in the wall boundary layer generated close to the sea bottom by the propagation of a monochromatic surface wave is determined by considering small values of both the wave steepness and the ratio between the thickness of the boundary layer and the local water depth. Depending on the hydrodynamic conditions, the sea bottom can be plane or rippled. The geometrical characteristics of the bottom forms are predicted using empirical formulae and, then, the bedforms are assumed to behave as a bottom roughness, the size of which is related to the size of the ripples. The bottom boundary layer is assumed to be turbulent and the flow field is computed by means of a two-equation turbulence model. Then the sediment transport is evaluated. The bed load is obtained using an empirical relationship. The suspended load is determined by computing the sediment flux, once the spatial and temporal distribution of sediment concentration is determined. A comparison of the model findings with the experimental results supports the approach.

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Section: The Numerical Solutioncontrasting

confidence: 52%

Sediment Transport at the Bottom of Sea Waves

Vittori

Blondeaux

2012

Int. Conf. Coastal. Eng.

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“…How close to shore streaming commences will vary with the wave field (Trowbridge & Madsen 1984, Kranenburg et al 2012, Henriquez et al 2014) and the slope of the bottom, but it is probably often present within tens to hundreds of meters of the shore (Fig. 12).…”

Section: Discussionmentioning

confidence: 99%

Transport of larvae and detritus across the surf zone of a steep reflective pocket beach

Shanks

MacMahan²,

Morgan³

et al. 2015

Mar. Ecol. Prog. Ser.

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“…The mechanism giving rise to the residual velocity is the asymmetry in turbulence intensity between the two flow half-cycles, which leads to the generation of a time-averaged, height-dependent stress within the boundary layer (Trowbridge & Madsen 1984;Davies & Li 1997;Holmedal & Myrhaug 2006). Figure 11 presents the residual velocity profiles for all of the present 12 experiments.…”

Section: Time-averaged Flowmentioning

confidence: 99%

Experimental study of the turbulent boundary layer in acceleration-skewed oscillatory flow

O’Donoghue

Davies

et al. 2011

J. Fluid Mech.

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Experiments have been conducted in a large oscillatory flow tunnel to investigate the effects of acceleration skewness on oscillatory boundary layer flow over fixed beds. As well as enabling experimental investigation of the effects of acceleration skewness, the new experiments add substantially to the relatively few existing detailed experimental datasets for oscillatory boundary layer flow conditions that correspond to full-scale sea wave conditions. Two types of bed roughness and a range of highReynolds-number, Re ∼ O(10 6 ), oscillatory flow conditions, varying from sinusoidal to highly acceleration-skewed, are considered. Results show the structure of the intrawave velocity profile, the time-averaged residual flow and boundary layer thickness for varying degrees of acceleration skewness, β. Turbulence intensity measurements from particle image velocimetry (PIV) and laser Doppler anemometry (LDA) show very good agreement. Turbulence intensity and Reynolds stress increase as the flow accelerates after flow reversal, are maximum at around maximum free-stream velocity and decay as the flow decelerates. The intra-wave turbulence depends strongly on β but period-averaged turbulent quantities are largely independent of β. There is generally good agreement between bed shear stress estimates obtained using the loglaw and using the momentum integral equation, and flow acceleration skewness leads to high bed shear stress asymmetry between flow half-cycles. Turbulent Reynolds stress is much less than the shear stress obtained from the momentum integral; analysis of the stress contributors shows that significant phase-averaged vertical velocities exist near the bed throughout the flow cycle, which lead to an additional shear stress, −ρũw; near the bed this stress is at least as large as the turbulent Reynolds stress.

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Turbulent wave boundary layers: 2. Second‐order theory and mass transport

Cited by 131 publications

References 13 publications

Sediment Transport at the Bottom of Sea Waves

Sediment Transport at the Bottom of Sea Waves

Transport of larvae and detritus across the surf zone of a steep reflective pocket beach

Experimental study of the turbulent boundary layer in acceleration-skewed oscillatory flow

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