# Bed stress assessment under solitary wave run-up

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## Abstract

Understanding and forecasting tsunami wave run-up is very important in mitigating tsunami hazards. The bed stress under wave motion governs viscous wave damping and sediment transport processes, which change coastal morphology. One of the most common methods used for simulation is the shallow water equation (SWE) model, often used with a Manning-style approach for modeling bottom friction. Boundary-layer approaches provide better information regarding bed stress, particularly since they are also valid for nonsteady flows. In this study, a simulation of wave run-up is carried out by simultaneous coupling of the SWE model with the *k*-*ω* model. The *k*-*ω* model is used near the flow boundary at the bottom, only for assessing the boundary layer shear stress. Free stream velocity and calculations of the free surface evolution are obtained from the SWE model. Both this method, and the conventional method, are applied to the canonical problem of a solitary wave propagating over a constant depth and then up a sloping beach (Synolakis, 1987). The new method is found to increase the computational accuracy and physical realism compared to the conventional Manning method. Comparison of bed shear stresses shows that the new method is able to accommodate the effect of deceleration, which leads to sign changes and a phase shift between the free stream velocity and the bed stress. Furthermore, it is found that during the run-up and run-down process, bed stress in the direction of leaving the shoreline is more dominant.

## Key words

Wave run-up numerical simulation shallow water equation boundary layer bed stress## 1. Introduction

The Great Tsunami of 2004 demonstrated the impact of tsunami waves both near and far (Geist et al., 2006). While flooding is a primary concern, tsunami waves cause large amounts of sediment transport, and drastically change the coastal morphology. They are also known to cause erosion, as seen in the East Java tsunami (Tsuji et al., 1995). Sediment transport processes under a wave motion are closely related to the bed shear stress, which is influenced by the boundary layer beneath the wave itself (Vittori and Blondeaux, 2008).

Studies of the evolution of tsunami waves are most often conducted using the long-wave approximation of the governing equations of motion. This study also uses numerical solutions and laboratory experiments. Synolakis (1987) conducted a series of laboratory experiments measuring the run-up of solitary waves. That study had a significant impact in the field, because he also provided analytical results for what he referred to as the canonical problem, i.e., a solitary wave propagating over a constant depth and then running up a sloping beach. His laboratory results are often used as benchmarks for validating numerical models.

There are several types of numerical models for the study of tsunami wave run-up. The SWE model is commonly used in tsunami wave run-up simulation and is known to model tsunami evolution well (Liu et al., 1991) and it is known for its computational efficiency, relatively good accuracy, and ease of modifying. Titov and Synolakis (1998) have used the SWE model to model a range of real tsunami inundation, including the 1993 Okushiri tsunami. More recently, Adityawan (2007) applied the SWE model to various cases of wave run up in shallow water, including the inundation of the 2004 tsunami in Banda Aceh, Indonesia. Nevertheless, the SWE model provides few details of the flow near the boundary. Variants of the Boussinesq equation (Boussinesq, 1872; Peregrine, 1967; Madsen and Sϕrensen, 1992; Nwogu, 1993; Wei and Kirby, 1995) have also been applied to various cases of wave run-up. Such models provide a higher accuracy than the SWE for shorter waves, but require more computation time and are not as flexible as the SWE in the treatment of alternating wet/dry and boundaries. Surprisingly, they have not been demonstrated to provide more accurate run-up predictions for tsunami run-up even for landslide waves (Lynett et al., 2003).

Two-dimensional (one horizontal and one vertical dimension) models have been proposed solving Reynolds Averaged Navier Stokes (RANS) with turbulence closure using a two-equation model, such as given by NEWFLUME (Lin, et al., 1999) or CADMAS SURF (Isobe, et al., 1999). Liu et al. (2005) proposed a full 3-D model using RANS. All such models adopt the VOF method and are able to reproduce the flow behavior in detail. However, they require exceptionally long computation times and are temperamental in terms of stability, and, hence, are so far fairly limited in the application to modeling analytical results or laboratory experiments. Other than possibly the case of landslide generated waves very nearshore, the Boussinesq and RANS models do no better in terms of inundation prediction than the SWE model, which enables implementation in practical applications, but is limited in its calculation of bottom shear stresses.

The SWE model consists of two simultaneous equations: conservation of mass (also known as continuity) and conservation of momentum. The empirical method of Manning is commonly used to evaluate bed shear stress. Because it was originally developed for steady river flow, the near-bed flows under wave motion cannot always be explained using the Manning approximation method. In nature, the bed stress changes its sign in a deceleration phase to a direction opposite to the free stream velocity, as shown by Liu et al. (2007). Yet, the Manning method calculates bed stress in the same direction as the velocity. It is clear that, for a detailed analysis, the Manning method is not sufficient.

There have been several studies of bed stress under wave motion. Tanaka (1988) estimated the bottom shear stress under non-linear waves by a modified stream function theory and proposed a formula to predict bed load transport, except near the surf zone in which acceleration effects play an important role. Furthermore, Tanaka and Thu (1994) have shown the importance of friction and phase differences between velocity and bed stress under waves, exactly where the Manning method fails to explain the switch. In general, more complete bed stress formulations may incorporate both velocity- and acceleration-related terms, or may include phase lag (e.g., Kabiling and Sato, 1993; Nielsen, 2002).

Suntoyo and Tanaka have used a boundary-layer approach to assess bed stress under solitary waves. They have demonstrated good accuracy of their bed stress approximation in numerical computations. Two-equation models are often used to assess the boundary-layer properties with *k*-*ϵ* and *k*-*ω* being the most common. The *k*-*ω* model has the ability to accommodate the roughness effects as bed boundary conditions and is considered to be more accurate in assessing the boundary-layer properties (Suntoyo, 2006). Adityawan et al. (2009) used a 2D *k*-*ω* model to investigate boundary-layer properties under a periodic sinusoidal wave motion, with good results.

The objective of this study is to assess bed stress under solitary wave run-up using a simultaneous coupling of SWE with a *k*-*ω* model. Each model is benchmarked with reference to a test case. Both models are coupled by replacing the conventional Manning method with a direct assessment of bed stress from the boundary layer using a *k*-*ω* model. Thus, bed stress can be approximated directly from the boundary layer using a *k*-*ω* model. The method is also used to simulate the canonical problem of Synolakis (1987). Further analyses are carried out regarding bed stress assessment.

## 2. Model Development

### 2.1 Coupling method

The governing equations are SWE and a *k*-*ω* equation. The models are calculated separately at each time step; however, their results are exchanged between the models, enabling a simultaneous calculation. The basic premise for the calculation is to upgrade the SWE model by replacing the Manning terms often used in the SWE using the direct calculation of bed stress in the near bed region using a *k*-*ω* model.

*k*-

*ω*model. Then, the bed stress obtained from the

*k*-

*ω*model is applied in the momentum equation of the SWE model for the next time step. The process continues until the end of the simulation, as shown in Fig. 1.

### 2.2 SWE model

*U*is the depth averaged velocity,

*t*is time,

*g*is gravity,

*z*

_{ b }is the bed elevation,

*ρ*is the fluid density and

*τ*

_{ o }is the bed stress. The Manning equation is commonly used to assess bed stress. The bed stress relation in the conventional Manning method is assumed to be proportional to the square of the velocity as shown below.where

*R*

_{ h }is the hydraulic radius, or can be considered to be the water depth for a very wide channel, and

*n*is the Manning roughness.

A wet-dry moving boundary condition is applied in the model to allow run-up simulation. A minimum threshold depth is selected. If the calculated water depth is lower than the threshold, then the water depth and velocity in the corresponding grid is given a zero value (dry cell).

*C*value is set to 0.99, and

*F*corresponds to the filtered parameters which are the velocity and depth.

### 2.3 The *k*-*ω* model

*k*-

*ω*model is based on the Reynolds-averaged equations of continuity and momentum:where

*u*

_{ i }and xi denotes the velocity in the boundary layer and location in the grid, Open image in new window is the fluctuating velocity in the

*x*(

*i*= 1) and

*y*(

*i*= 2) directions,

*P*is the static pressure,

*v*is the kinematic viscosity. Open image in new window is the Reynolds stress tensor, and

*S*

_{ i j }is the strain-rate tensor from the followingequation:The Reynolds stress tensor is given through eddy viscosity by a Boussinesq approximation:where

*k*is the turbulent kinetic energy and

*δ*

_{ i j }is the Kro-necker delta. The turbulent kinetic energy and specific dissipation rate,

*ω*in the

*k*-

*ω*model equation, is given as follows:The eddy viscosity is given byThe values of the closure coefficients are given by Wilcox (1988) as

*β*= 3/40,

*β** = 0.09,

*α*= 5/9, and

*σ*=

*σ** = 0.5. The boundary condition at the bottom is no slip boundary. At the free stream, it is assumed that the velocity gradient, the turbulent kinetic energy gradient and the dissipation rate gradient are zero. The governing equations above are solved using a Crank-Nicolson-type implicit finite-difference scheme. More details regarding the scheme implementation can be found in a previous study (Suntoyo et al., 2008).

## 3. Numerical Simulation

The developed method consists of two different models. Each model is verified for an appropriate case. The *k*-*ω* model is used to simulate the bed stress fluctuation under random waves. The SWE model is used to simulate the run-up case.

### 3.1 *k*-*ω* model verification

*k*-

*ω*model is verified using measurement data of random waves in a flume. Bed stress measurements were conducted using a hot film sensor. Details of the experiment can be found in a previous study by Tanaka et al. (1998). The data sets consist of free stream velocity and bed stress over time. Bed stress measurements were made using a very thin layer film. The measured velocity data is used to calculate the pressure gradient which is applied as the model input. The simulation is conducted to obtain the bed stress. In this case, a 1D model is used to cover the boundary-layer do-main within a vertical direction. The water depth 0.1 meter above the bed is taken to ensure that the pressure gradient is applied outside the boundary layer. The vertical grid size is 0.0004 meter. The simulation is conducted with a time step of 0.001 second for 25 seconds. The bed shear stress measurement and the simulation result is shown in Fig. 3. The simulation shows a good comparison with the measurement data. Similar behaviour is also observed between the data and simulation result.

### 3.2 SWE model verification

*n*) for the simulation was determined by trial and error. A Manning value of (

*n*) 0.043 was found to provide the best results. The second model is the upgraded SWE model using the new method proposed in this study. The model setup for this case is shown in Fig. 4.

*h*

_{ o }is the initial water depth,

*η*is the water elevation,

*x*is the coordinate as shown in the model sketch. An asterisk denotes the corresponding parameter in non-dimensional form.

*U*

_{ c }is given asThe grid size in the

*x*direction for both models is 0.1

*x**. The time step for both models is 0.001

*t**. It should be noted here that the Manning method is able to provide an accurate result using a time step of 0.1

*t**. However, the new method requires a much finer time step due to the finer grid in the vertical direction. The grid size in the vertical direction is 0.0005 m. In the experiment, the ratio of the initial wave height to the depth is 0.019 with a beach slope of 1:19.85.The incoming solitary wave Reynolds number (

*R*

_{ E }) is 1600, which can be calculated with the following equation:where

*U*

_{ c }is the maximum of the free stream velocity,

*a*

_{ m }is half of the stroke of water particle displacement. The Reynolds number was found to be much smaller than the transition Reynolds numbers (2 × 10

^{5}<

*R*

_{ E }< 5 × 10

^{5}) as proposed by Sumer et al. (2010). Thus, the incoming wave is considered a laminar condition.

*X*

_{1}which is situated at half of the initial wave length (

*L*/2) from the initial slope (

*X*

_{0}). The wave length (

*L*) can be calculated with the following equation:The new method is applied to a grid with a water depth higher than 1.2 cm. If the water depth is lower than 1.2 cm, the bed stress is calculated from the momentum equation.

*R*is the estimated run-up height and

*ϕ*is the bed slope.

Run-up height.

| Square error | |||||
---|---|---|---|---|---|---|

MM | NM | MM | NM | |||

Cot | (1) | (2) | (3) | ((1)–(2)) | ((1)–(3)) | |

19.85 | 0.089 | 0.069 | 0.078 | 0.000407 | 0.000116 | |

11.43 | 0.068 | 0.064 | 0.063 | 0.000016 | 0.000017 | |

10.00 | 0.063 | 0.059 | 0.067 | 0.000017 | 0.000015 | |

5.67 | 0.048 | 0.045 | 0.050 | 0.000004 | 0.000004 | |

5.00 | 0.045 | 0.043 | 0.046 | 0.000002 | 0.000001 | |

3.73 | 0.039 | 0.036 | 0.037 | 0.000008 | 0.000003 | |

RMSE | 0.008704 | 0.005404 |

## 4. Bed Stress Assessment

*t*, with Open image in new window and Open image in new window corresponding to negative and positive bed stress values, respectively.

*T*is the simulation time, with

*T*

_{(+)}and

*T*

_{(−)}corresponding to the period length of positive and negative bed stress, respectively.

*t*is the corresponding time of the calculated bed stress, with

*T*

_{(+)}and

*T*

_{(−)}denoting the time where the bed stress is positive and negative, respectively. Negative and positive signs denotes the direction towards, or leaving, the shoreline, respectively. The maximum ( Open image in new window ) and minimum ( Open image in new window ) value of non-dimensional bed stress is also investigated.

## 5. Conclusion

An assessment of the bed shear stress under a solitary wave run-up was carried out in this study, using the conventional Manning method, and a new method based on the *k*-*ω* equations. Both methods were used to simulate the evolution of solitary waves for the canonical problem of Synolakis (1987) for a non-breaking wave condition, with satisfactory results. Comparisons of run-up heights and detailed free surface profiles particular at the moving shoreline, show that the new method exhibits smaller deviations, compared with laboratory measurements, than the Manning method. This is perhaps to be expected, since the Manning method was developed for steady unidirectional flows, and cannot reproduce well the bed stress under a wave motion, except with ad-hoc assumptions. The Manning method fails to explain the phase shift of the velocity peak to the bed stress. It also fails to predict the change of sign during the deceleration phase in the solitary wave profile. The method proposed in this study is able to assess bed stress behavior under wave motion. Bed stress comparisons between the Manning method and the new method shows that the Manning method tends to higher magnitudes in a shallow area and lower magnitudes in deeper areas. Further analysis of bed stress accumulation shows that the bed stress away from the shoreline will be more dominant during the entire runup process.

## Notes

### Acknowledgments

This research was supported by Grant-in-Aid for Scientific Research from the Japan Society for the Promotion of Science (No. 22360193), and partially supported by the Open Fund for Scientific Research from the State Key Laboratory of Hydraulics and Mountain River Engineering, Sichuan University, China. The first author is a scholarship holder under the auspices of the Indonesian Ministry of Education. The authors would also like to thank Professor Synolakis and an anonymous reviewer for their constructive review of the present paper.

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