# Theoretical and Experimental Investigations of Wave-Induced Vertical Mixing

Authors: Wojciech Sulisz; Maciej Paprota
Journal: Mathematical Problems in Engineering
 (2015)

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## Abstract

Theoretical investigations supported by a series of original laboratory experiments are conducted to study a wave-induced vertical mixing process. The derived semi-analytical solution is very efficient and is applied to predict the effects of water waves on the temperature changes and the evolution of temperature profiles. The results indicate that waves increase a mixing process. The rate of change of the temperature is higher when waves contributed to mixing process and this process increases with increasing the wavelength to water depth ratio. The analysis indicates that for typical ocean waves the contribution of water waves to mixing may be several orders of magnitude higher than a corresponding contribution arising from the classical diffusion process. This implies a need to conduct more theoretical studies and experimental investigation on the effect of water waves on mixing processes. A series of original laboratory experiments were conducted in the insulated wave flume to verify the derived model. The comparisons show a reasonable agreement between predicted and measured temperature profiles. A reasonable agreement between theoretical results and experimental data is observed for the whole considered range of initial temperature distributions. The comparisons indicate that the model is applicable even to cases when gradients in temperature distributions over water depth are fairly high.


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## Body

## 1. Introduction

A wave-induced mixing is an important process from a practical point of view and is a challenging problem for theoretical investigations. The understanding of wave-induced mixing is one of the main tasks of physical oceanographers and climatologists and is of fundamental importance for the modeling and an accurate prediction of ocean transport processes and climate changes.Water waves are the result of a dynamic process at the intersection of the atmosphere and ocean and constitute one of the largest sources of energy in the ocean [1–3]. Terawatts of energy of water waves imply that waves have a significant effect on ocean processes. In recent decades the influence of waves on transport processes has become even more significant due to increasing number of severe storms occurring mainly in the Northeast Pacific and the North Atlantic [4–6] as a result of climate change [7, 8]. Theoretical investigations and field observations have shown that waves affect the exchanges of momentum, heat, and masses in the upper oceans and that wave-induced processes lead to vertical mixing in the ocean [9]. The mixing has been attributed to wave breaking process [10–12]. It has been shown that wave energy dissipated through wave breaking enhances turbulence intensity near the sea surface and mixing [10, 13–15].Although it is recognized that waves affect a vertical mixing, the complexity of wave-induced processes in the upper ocean causes that the mixing is attributed to wave breaking phenomena. However, the strong turbulence induced by wave breaking is mainly confined within the near-surface zone with the depth scale of wave heights [11, 16, 17] and it is hard to justify why this small layer has such a big effect on the upper oceans. It is expected that the whole process is significantly affected by nonbreaking waves which can transport turbulence and increase mixing. Numerical experiments conducted by implementing parameterized wave-induced mixing in ocean circulation models and climate models indicate a significant effect of mixing on ocean circulation and climate predictions and a necessity to study mixing induced by nonbraking waves [18–21]. The role of nonbreaking waves in vertical mixing needs further investigations and fundamental research.Laboratory experiments have been shown to be an efficient method in the investigations of hydrodynamic and thermodynamic problems. Wave-induced mixing processes can be studied in laboratories by conducting experiments in a wave flume. This type of approach has been shown to be indispensable in the studies of many wave-induced processes [22]. The repeatable experiments in the well-controlled environment of a wave flume enable us to perform an accurate investigation that is essential in the analysis of the physics of wave-induced mixing phenomenon. Moreover, a laboratory investigation provides useful data for the analysis of the correlations between spectral and statistical characteristics of wave regimes and wave-induced mixing process. Finally, laboratory experiments enable us to avoid some side effects and separate the mixing originated from breaking and nonbreaking process, which is of fundamental importance for the understanding of mixing processes and an accurate calibration and verification of numerical models.In this work theoretical studies and laboratory experiments are conducted to investigate a wave-induced mixing process. First, theoretical investigations are conducted to provide insight into a potential origin of a wave-induced mixing. Then, a series of laboratory experiments are conducted to investigate wave-induced vertical mixing. Experimental data are analyzed with the emphasis on factors and wave parameters affecting mixing process. Finally, the theoretical results are compared with experimental data and conclusions are specified.


## 2. Theory

### 2.1. Particle Kinematics

We consider the propagation of nonlinear water waves in a periodic uniform wave train and their potential effect on wave-induced mixing. A right-hand Cartesian coordinate system is selected such that thexy plane is horizontal and coincides with the undisturbed free surface and z points vertically upwards (Figure 1).Figure 1
Definitions sketch and coordinate systems.The following are assumed:(i)
The fluid is inviscid and incompressible.(ii)
The fluid motion is irrotational.(iii)
The sea bottom is impervious.According to the assumptions the velocity vector,V(x,z,t), has a potential Φ(x,z,t), such that V=∇Φ. The fluid motion is governed by the Laplace equation(1a)∇2Φ=0and the Bernoulli equation(1b)Φt+1ρP+gz+12∇Φ2=0,where ρ is the fluid density, P is the pressure, and g is the acceleration due to gravity.The velocity potential,Φ(x,z,t), satisfies the Laplace equation(2a)∇2Φ=0.At the free surface the velocity potential, Φ(x,z,t), has to satisfy the kinematic boundary condition(2b)ηt+Φxηx-Φz=0,z=ηx,t,and the dynamic boundary condition(2c)Φt+gη+12∇Φ2=0,z=ηx,t.At the wavemaker the velocity potential, Φ(x,z,t), has to satisfy the kinematic boundary condition(2d)χt+Φzχz-Φx=0,x=χz,t.At the sea bottom the following boundary condition must be satisfied:(2e)Φz=0,z=-h.Moreover, the velocity potential must satisfy boundary conditions at infinity and initial conditions [23].A solution of the boundary-value problem, (2a), (2b), (2c), (2d), and (2e), is not a trivial task. It is difficult to find the velocity potential which satisfies the free-surface boundary conditions, because the boundary conditions contain nonlinear terms. Additional difficulties arise from a need to apply the boundary conditions on the free surface which is unknown and is a part of a final solution [23]. In order to achieve a solution, the kinematic free-surface boundary condition and the dynamic free-surface boundary condition are often expanded in a Taylor series about a mean position:(3a)∑n=0∞ηnn!∂n∂znηt+Φxηx-Φz=0,z=0,(3b)∑n=0∞ηnn!∂n∂znΦt+gη+12∇Φ2=0,z=0,(3c)∑n=0∞χnn!∂n∂xnχt+Φzχz-Φx=0,x=0,which usually helps to obtain a solution [24, 25].By expanding the kinematic free-surface boundary condition and the dynamic free-surface boundary condition in a Taylor series and collecting terms up to third order in wave amplitude, one obtains the following boundary-value problem:(4a)∇2Φ=0,(4b)∂η∂t+∂Φ∂x∂η∂x-∂Φ∂z+η∂2Φ∂x∂z∂η∂x-η∂2Φ∂z2-12η2∂3Φ∂z3=0,z=0,(4c)∂Φ∂t+gη+12∂Φ∂x2+∂Φ∂z2+η∂2Φ∂z∂t+η∂Φ∂x∂2Φ∂x∂z+∂Φ∂z∂2Φ∂z2+12η2∂3Φ∂z2∂t=0,z=0,(4d)∂χ∂t+∂Φ∂z∂χ∂z-∂Φ∂x+χ∂2Φ∂z∂x∂χ∂z-χ∂2Φ∂x2+12χ2∂3Φ∂z∂x2∂χ∂z-12χ2∂3Φ∂x3=0,x=0,(4e)Φz=0,z=-h.Moreover, the velocity potential must satisfy boundary conditions at infinity and initial conditions [23].For weakly nonlinear waves the solutions of the boundary-value problem, (4a), (4b), (4c), (4d), and (4e), can be obtained by applying a perturbation method [26, 27]. The solution is becoming complicated by increasing the number of terms applied in the perturbation method. The basic solution may be written in the following form:(5a)Φx,z,t=Agωcosh⁡kz+hcosh⁡khsin⁡kx-ωt+38ωA2cosh⁡2kz+hsinh4⁡khsin⁡2kx-ωtηx,t=Acos⁡kx-ωt+14A2kcosh⁡khsinh3⁡kh2+cosh⁡2khcos⁡2kx-ωt,provided that(5b)ω2g=tanh⁡kh,where A is the wave amplitude, k is the wave number, ω is the frequency, and h is the water depth.For waves of moderate steepness and steep waves a solution of the boundary-value problem, (4a), (4b), (4c), (4d), and (4e), can be obtained by applying a semi-analytical technique. A solution procedure is complicated because of a need to satisfy the kinematic wavemaker boundary condition. In order to obtain a solution the velocity potential, Φ, is expressed as a linear combination of two velocity potentials Φf and Φw. The velocity potential Φf is introduced to satisfy the free-surface boundary conditions and the velocity potential Φw is introduced to satisfy the wavemaker kinematic boundary condition. As a consequence the solution may be sought in the following form:(6a)Φfx,z,t=∑n=0Ancosh⁡λnz+hcosh⁡λnhcos⁡λnx(6b)Φwx,z,t=B0x-b2+z+h2+∑m=1Bmcosh⁡μmx-bcosh⁡μmbcos⁡μmz+h(6c)ηx,t=∑n=0ancos⁡λnx,where(6d)λn=nπb,(6e)μm=mπh,in which An, Bm, and an are functions of time and b is the length of a computational domain. The solution in the form of the eigenfunction expansions, (6a), (6b), (6c), (6d), and (6e), satisfies the Laplace equation and the bottom boundary condition. A time-stepping procedure is applied to satisfy the remaining boundary conditions (4b) and (4c) and to determine the unknown coefficients of the eigenfunction expansions. The time-stepping procedure is based on the Adams-Bashforth-Moulton predictor-corrector method [28]. The method enables prediction of the value of a function f from its time derivatives f′. According to the solution procedure, the Adams-Bashforth predictor(7a)fn+1=fn+Δt2455fn′-59fn-1′+37fn-2′-9fn-3′is combined with the Adams-Moulton corrector(7b)fn+1=fn+Δt249fn+1′+19fn′-5fn-1′+fn-2′and with the free-surface boundary conditions (4b) and (4c) to predict the free-surface elevation η and the velocity potential Φ at a new time step.


### 2.2. Modeling of Mixing

The equation for temperature diffusion can be written in the following form:(8)∂T∂t-∂∂zκ∂T∂z=0,where T denotes the water temperature, κ is the vertical diffusion coefficient, t is the time, and z is the vertical coordinate.A theoretical analysis indicates that the vertical diffusion coefficient may be written in the form of a sum of the molecular and wave-induced diffusivities:(9)κ=κm+κV,where κm=1.4·10-7 m2/s is the background molecular diffusivity and κV represents the wave-induced diffusivity.There are several possibilities to assessκV. In the present studies the Prandtl mixing length hypothesis is applied to calculate the wave-induced diffusivity. By applying the Prandtl mixing length approach the wave-induced diffusivity may be calculated from (10)κV=lw′,where l is the mixing length and w′ is the increment of the vertical velocity.Since the increment of the velocity in the vertical direction can be expressed as(11)w′=l∂ww0.5∂zthe formula for the wave-induced diffusivity may be written in the following form: (12)κV=l2∂ww0.5∂z.For weakly nonlinear waves it is reasonable to assume that the mixing length l is proportional to the particle displacement in the vertical direction. Since the mixing length l is proportional to the wave particle displacement, the product l2 may be written as follows:(13)l2∝A2sinh2⁡kz+hsinh2⁡kh.Finally, by substituting (13) into (12) and conducting simple derivations, the formula for the wave-induced diffusivity may be written as (14)κV=αA3kωsinh2⁡kz+hcosh⁡kz+hsinh3⁡kh,where α is the dimensionless coefficient which should be determined by observations or numerical experiments. In previous studies, due to the lack of information on the value of this coefficient, its value was assumed to be 1 by default. In Figure 2 the wave-induced diffusivity calculated using (14) for different wave cases is presented.Figure 2
Wave-induced diffusivity for weakly nonlinear waves.For waves of moderate steepness and steep waves the wave-induced diffusivity was calculated by applying the derived nonlinear wave model and the formula (12). The mean values in (12) of the square of wave particle displacement and vertical derivative of square root of the product of vertical velocity component were calculated by integrating these quantities over a finite number of wave periods of regular waves. In Figure 3 the wave-induced diffusivity calculated for waves of moderate steepness and steep waves for different wave cases is presented.Figure 3
Wave-induced diffusivity for waves of moderate steepness and steep waves atx/h=6.The plots in Figures2 and 3 show that for waves of small and moderate steepness nonlinear effects are of secondary importance and a weakly nonlinear wave theory can be applied to determine a wave-induced diffusivity. For steeper waves, nonlinear wave effects and the effects arising from the interaction of wave components are becoming more and more important and a nonlinear approach must be applied to calculate a wave-induced diffusivity.The closed-form expression derived for the wave-induced diffusivity enables us to incorporate water waves in a mixing process. As a consequence, the temperature in the water column and its evolution must satisfy(15a)∂T∂t-∂∂zκ∂T∂z=0,at the free water surface (15b)νT-∂T∂z=0,z=0,and at the bottom(15c)∂T∂z=0,z=-h,provided that (15d)Tz=T0z,t=0,where T0(z) is assumed to be the known temperature distribution in the water column at t=0. The condition at z=0 accounts for a partial radiation at the water surface. This type of conditions is widely applied in the modelling of many physical phenomena. In general, ν may be a complex-value quantity, which often facilitates modelling process.The solution of (15a), (15b), (15c), and (15d) is achieved by a time-stepping procedure and applying an eigenfunction expansion method to describe T and the Adams-Bashforth-Moulton formulas to proceed in time [28]. This method has been shown to be an efficient technique in the modeling of the propagation and transformation of nonlinear water waves [22, 29]. Accordingly, the solution has the following form:(16a)T=∑n=1Nantcos⁡λnz+h,provided that the eigenvalues satisfy (16b)ν+λntan⁡λnh=0.The coefficients of the eigenfunction expansions are determined by applying a Fourier method. The application of the eigenfunction expansions and a Fourier method makes the solution procedure a very efficient technique and enables us to obtain results even for large spatial or time domains.The wave-induced diffusivity, (14), has been derived for the first time and enables us to eventually evaluate the role of surface waves in mixing process. The derivation is based on the Prandtl mixing length hypothesis. Because of uncertainties related with possibilities to apply the Prandtl mixing length hypothesis to adequately describe the wave-induced diffusivity and the lack of solid evidence on its applicability range, experimental verification of the proposed model seems to be a must. This is why in this study laboratory experiments are conducted to provide insight into mixing process and eventually supply experimental data to verify the derived model.


## 2.1. Particle Kinematics

We consider the propagation of nonlinear water waves in a periodic uniform wave train and their potential effect on wave-induced mixing. A right-hand Cartesian coordinate system is selected such that thexy plane is horizontal and coincides with the undisturbed free surface and z points vertically upwards (Figure 1).Figure 1
Definitions sketch and coordinate systems.The following are assumed:(i)
The fluid is inviscid and incompressible.(ii)
The fluid motion is irrotational.(iii)
The sea bottom is impervious.According to the assumptions the velocity vector,V(x,z,t), has a potential Φ(x,z,t), such that V=∇Φ. The fluid motion is governed by the Laplace equation(1a)∇2Φ=0and the Bernoulli equation(1b)Φt+1ρP+gz+12∇Φ2=0,where ρ is the fluid density, P is the pressure, and g is the acceleration due to gravity.The velocity potential,Φ(x,z,t), satisfies the Laplace equation(2a)∇2Φ=0.At the free surface the velocity potential, Φ(x,z,t), has to satisfy the kinematic boundary condition(2b)ηt+Φxηx-Φz=0,z=ηx,t,and the dynamic boundary condition(2c)Φt+gη+12∇Φ2=0,z=ηx,t.At the wavemaker the velocity potential, Φ(x,z,t), has to satisfy the kinematic boundary condition(2d)χt+Φzχz-Φx=0,x=χz,t.At the sea bottom the following boundary condition must be satisfied:(2e)Φz=0,z=-h.Moreover, the velocity potential must satisfy boundary conditions at infinity and initial conditions [23].A solution of the boundary-value problem, (2a), (2b), (2c), (2d), and (2e), is not a trivial task. It is difficult to find the velocity potential which satisfies the free-surface boundary conditions, because the boundary conditions contain nonlinear terms. Additional difficulties arise from a need to apply the boundary conditions on the free surface which is unknown and is a part of a final solution [23]. In order to achieve a solution, the kinematic free-surface boundary condition and the dynamic free-surface boundary condition are often expanded in a Taylor series about a mean position:(3a)∑n=0∞ηnn!∂n∂znηt+Φxηx-Φz=0,z=0,(3b)∑n=0∞ηnn!∂n∂znΦt+gη+12∇Φ2=0,z=0,(3c)∑n=0∞χnn!∂n∂xnχt+Φzχz-Φx=0,x=0,which usually helps to obtain a solution [24, 25].By expanding the kinematic free-surface boundary condition and the dynamic free-surface boundary condition in a Taylor series and collecting terms up to third order in wave amplitude, one obtains the following boundary-value problem:(4a)∇2Φ=0,(4b)∂η∂t+∂Φ∂x∂η∂x-∂Φ∂z+η∂2Φ∂x∂z∂η∂x-η∂2Φ∂z2-12η2∂3Φ∂z3=0,z=0,(4c)∂Φ∂t+gη+12∂Φ∂x2+∂Φ∂z2+η∂2Φ∂z∂t+η∂Φ∂x∂2Φ∂x∂z+∂Φ∂z∂2Φ∂z2+12η2∂3Φ∂z2∂t=0,z=0,(4d)∂χ∂t+∂Φ∂z∂χ∂z-∂Φ∂x+χ∂2Φ∂z∂x∂χ∂z-χ∂2Φ∂x2+12χ2∂3Φ∂z∂x2∂χ∂z-12χ2∂3Φ∂x3=0,x=0,(4e)Φz=0,z=-h.Moreover, the velocity potential must satisfy boundary conditions at infinity and initial conditions [23].For weakly nonlinear waves the solutions of the boundary-value problem, (4a), (4b), (4c), (4d), and (4e), can be obtained by applying a perturbation method [26, 27]. The solution is becoming complicated by increasing the number of terms applied in the perturbation method. The basic solution may be written in the following form:(5a)Φx,z,t=Agωcosh⁡kz+hcosh⁡khsin⁡kx-ωt+38ωA2cosh⁡2kz+hsinh4⁡khsin⁡2kx-ωtηx,t=Acos⁡kx-ωt+14A2kcosh⁡khsinh3⁡kh2+cosh⁡2khcos⁡2kx-ωt,provided that(5b)ω2g=tanh⁡kh,where A is the wave amplitude, k is the wave number, ω is the frequency, and h is the water depth.For waves of moderate steepness and steep waves a solution of the boundary-value problem, (4a), (4b), (4c), (4d), and (4e), can be obtained by applying a semi-analytical technique. A solution procedure is complicated because of a need to satisfy the kinematic wavemaker boundary condition. In order to obtain a solution the velocity potential, Φ, is expressed as a linear combination of two velocity potentials Φf and Φw. The velocity potential Φf is introduced to satisfy the free-surface boundary conditions and the velocity potential Φw is introduced to satisfy the wavemaker kinematic boundary condition. As a consequence the solution may be sought in the following form:(6a)Φfx,z,t=∑n=0Ancosh⁡λnz+hcosh⁡λnhcos⁡λnx(6b)Φwx,z,t=B0x-b2+z+h2+∑m=1Bmcosh⁡μmx-bcosh⁡μmbcos⁡μmz+h(6c)ηx,t=∑n=0ancos⁡λnx,where(6d)λn=nπb,(6e)μm=mπh,in which An, Bm, and an are functions of time and b is the length of a computational domain. The solution in the form of the eigenfunction expansions, (6a), (6b), (6c), (6d), and (6e), satisfies the Laplace equation and the bottom boundary condition. A time-stepping procedure is applied to satisfy the remaining boundary conditions (4b) and (4c) and to determine the unknown coefficients of the eigenfunction expansions. The time-stepping procedure is based on the Adams-Bashforth-Moulton predictor-corrector method [28]. The method enables prediction of the value of a function f from its time derivatives f′. According to the solution procedure, the Adams-Bashforth predictor(7a)fn+1=fn+Δt2455fn′-59fn-1′+37fn-2′-9fn-3′is combined with the Adams-Moulton corrector(7b)fn+1=fn+Δt249fn+1′+19fn′-5fn-1′+fn-2′and with the free-surface boundary conditions (4b) and (4c) to predict the free-surface elevation η and the velocity potential Φ at a new time step.


## 2.2. Modeling of Mixing

The equation for temperature diffusion can be written in the following form:(8)∂T∂t-∂∂zκ∂T∂z=0,where T denotes the water temperature, κ is the vertical diffusion coefficient, t is the time, and z is the vertical coordinate.A theoretical analysis indicates that the vertical diffusion coefficient may be written in the form of a sum of the molecular and wave-induced diffusivities:(9)κ=κm+κV,where κm=1.4·10-7 m2/s is the background molecular diffusivity and κV represents the wave-induced diffusivity.There are several possibilities to assessκV. In the present studies the Prandtl mixing length hypothesis is applied to calculate the wave-induced diffusivity. By applying the Prandtl mixing length approach the wave-induced diffusivity may be calculated from (10)κV=lw′,where l is the mixing length and w′ is the increment of the vertical velocity.Since the increment of the velocity in the vertical direction can be expressed as(11)w′=l∂ww0.5∂zthe formula for the wave-induced diffusivity may be written in the following form: (12)κV=l2∂ww0.5∂z.For weakly nonlinear waves it is reasonable to assume that the mixing length l is proportional to the particle displacement in the vertical direction. Since the mixing length l is proportional to the wave particle displacement, the product l2 may be written as follows:(13)l2∝A2sinh2⁡kz+hsinh2⁡kh.Finally, by substituting (13) into (12) and conducting simple derivations, the formula for the wave-induced diffusivity may be written as (14)κV=αA3kωsinh2⁡kz+hcosh⁡kz+hsinh3⁡kh,where α is the dimensionless coefficient which should be determined by observations or numerical experiments. In previous studies, due to the lack of information on the value of this coefficient, its value was assumed to be 1 by default. In Figure 2 the wave-induced diffusivity calculated using (14) for different wave cases is presented.Figure 2
Wave-induced diffusivity for weakly nonlinear waves.For waves of moderate steepness and steep waves the wave-induced diffusivity was calculated by applying the derived nonlinear wave model and the formula (12). The mean values in (12) of the square of wave particle displacement and vertical derivative of square root of the product of vertical velocity component were calculated by integrating these quantities over a finite number of wave periods of regular waves. In Figure 3 the wave-induced diffusivity calculated for waves of moderate steepness and steep waves for different wave cases is presented.Figure 3
Wave-induced diffusivity for waves of moderate steepness and steep waves atx/h=6.The plots in Figures2 and 3 show that for waves of small and moderate steepness nonlinear effects are of secondary importance and a weakly nonlinear wave theory can be applied to determine a wave-induced diffusivity. For steeper waves, nonlinear wave effects and the effects arising from the interaction of wave components are becoming more and more important and a nonlinear approach must be applied to calculate a wave-induced diffusivity.The closed-form expression derived for the wave-induced diffusivity enables us to incorporate water waves in a mixing process. As a consequence, the temperature in the water column and its evolution must satisfy(15a)∂T∂t-∂∂zκ∂T∂z=0,at the free water surface (15b)νT-∂T∂z=0,z=0,and at the bottom(15c)∂T∂z=0,z=-h,provided that (15d)Tz=T0z,t=0,where T0(z) is assumed to be the known temperature distribution in the water column at t=0. The condition at z=0 accounts for a partial radiation at the water surface. This type of conditions is widely applied in the modelling of many physical phenomena. In general, ν may be a complex-value quantity, which often facilitates modelling process.The solution of (15a), (15b), (15c), and (15d) is achieved by a time-stepping procedure and applying an eigenfunction expansion method to describe T and the Adams-Bashforth-Moulton formulas to proceed in time [28]. This method has been shown to be an efficient technique in the modeling of the propagation and transformation of nonlinear water waves [22, 29]. Accordingly, the solution has the following form:(16a)T=∑n=1Nantcos⁡λnz+h,provided that the eigenvalues satisfy (16b)ν+λntan⁡λnh=0.The coefficients of the eigenfunction expansions are determined by applying a Fourier method. The application of the eigenfunction expansions and a Fourier method makes the solution procedure a very efficient technique and enables us to obtain results even for large spatial or time domains.The wave-induced diffusivity, (14), has been derived for the first time and enables us to eventually evaluate the role of surface waves in mixing process. The derivation is based on the Prandtl mixing length hypothesis. Because of uncertainties related with possibilities to apply the Prandtl mixing length hypothesis to adequately describe the wave-induced diffusivity and the lack of solid evidence on its applicability range, experimental verification of the proposed model seems to be a must. This is why in this study laboratory experiments are conducted to provide insight into mixing process and eventually supply experimental data to verify the derived model.


## 3. Laboratory Experiments

### 3.1. Wave Flume

Laboratory experiments were conducted in the wave flume at the Institute of Hydroengineering, Polish Academy of Sciences, Gdańsk. The wave flume at the Institute of Hydroengineering is 64 m long and 1.4 m deep. It is equipped with a programmable piston wave generator. The experiments were performed in a separated section of the wave flume of the widthb=0.3 m shown schematically in Figure 4. The water depth in the wave flume was h=0.4 m. A system of electrical heaters was immersed into the upper water layer and the water was heated up. Then, the system of heaters was lifted and the flume was fully covered by insulation plates. The temperature was measured by a temperature gauge. The temperature sensor was installed on a measuring rod to precisely identify its vertical position. The measurements were performed with the maximum absolute error of 0.1°C for temperature registration and 0.0001 m for location. The distance from the temperature gauge to the wavemaker was x=1.3 m. Final experiments and temperature records were preceded by a series of control measurements in the horizontal and vertical directions.Figure 4
Side and top view of the wave flume.In the first series of laboratory experiments investigations focused on temperature diffusion for still water conditions. Laboratory experiments were performed in the insulated wave flume shown schematically in Figure4. A system of electrical heaters was immersed 0.12 m into the upper water layer and the water was heated up. Then, the temperature profile over depth was measured. The measurements were conducted every 0.01 m. After approximately one hour the temperature profile was measured again to record changes of temperature due to diffusion and heat losses. The experiments were repeated for two different initial temperature profiles to provide more data for the verification of the derived model. In the first case the measurements started when the temperature at the free surface reached 33.2°C and in the second case, intended to include profiles of lower temperature gradients, the measurements started at 27.8°C.In the second series of laboratory experiments the investigations focused on the effect of surface waves on the vertical mixing process. Laboratory experiments were performed in the same insulated section of the wave flume as previous series of experiments. A system of electrical heaters was used to heat up the upper water layer in the wave flume. Then, the temperature profile over depth was measured. The measurements were conducted every 0.01 m. After the measurement of the temperature profile was finished, a train of regular waves was generated. When waves and internal waves decayed, the temperature profile over depth was measured again to provide information on the effect of surface waves on vertical mixing process. The experiments were repeated for two different scenarios to provide more data for the verification of the derived model. In the first case the wavemaker generated deep-water waves for 105 s withA1/h=0.065, L/h=2 and in the second case waves were generated for 120 s with A1/h=0.07, L/h=4. Water waves considered in the first case are typical deep-water waves. Waves in the second case, higher and longer, were included in the experimental program intentionally, because these waves were expected to have more pronounced effect on mixing than waves in the first case.


## 3.1. Wave Flume

Laboratory experiments were conducted in the wave flume at the Institute of Hydroengineering, Polish Academy of Sciences, Gdańsk. The wave flume at the Institute of Hydroengineering is 64 m long and 1.4 m deep. It is equipped with a programmable piston wave generator. The experiments were performed in a separated section of the wave flume of the widthb=0.3 m shown schematically in Figure 4. The water depth in the wave flume was h=0.4 m. A system of electrical heaters was immersed into the upper water layer and the water was heated up. Then, the system of heaters was lifted and the flume was fully covered by insulation plates. The temperature was measured by a temperature gauge. The temperature sensor was installed on a measuring rod to precisely identify its vertical position. The measurements were performed with the maximum absolute error of 0.1°C for temperature registration and 0.0001 m for location. The distance from the temperature gauge to the wavemaker was x=1.3 m. Final experiments and temperature records were preceded by a series of control measurements in the horizontal and vertical directions.Figure 4
Side and top view of the wave flume.In the first series of laboratory experiments investigations focused on temperature diffusion for still water conditions. Laboratory experiments were performed in the insulated wave flume shown schematically in Figure4. A system of electrical heaters was immersed 0.12 m into the upper water layer and the water was heated up. Then, the temperature profile over depth was measured. The measurements were conducted every 0.01 m. After approximately one hour the temperature profile was measured again to record changes of temperature due to diffusion and heat losses. The experiments were repeated for two different initial temperature profiles to provide more data for the verification of the derived model. In the first case the measurements started when the temperature at the free surface reached 33.2°C and in the second case, intended to include profiles of lower temperature gradients, the measurements started at 27.8°C.In the second series of laboratory experiments the investigations focused on the effect of surface waves on the vertical mixing process. Laboratory experiments were performed in the same insulated section of the wave flume as previous series of experiments. A system of electrical heaters was used to heat up the upper water layer in the wave flume. Then, the temperature profile over depth was measured. The measurements were conducted every 0.01 m. After the measurement of the temperature profile was finished, a train of regular waves was generated. When waves and internal waves decayed, the temperature profile over depth was measured again to provide information on the effect of surface waves on vertical mixing process. The experiments were repeated for two different scenarios to provide more data for the verification of the derived model. In the first case the wavemaker generated deep-water waves for 105 s withA1/h=0.065, L/h=2 and in the second case waves were generated for 120 s with A1/h=0.07, L/h=4. Water waves considered in the first case are typical deep-water waves. Waves in the second case, higher and longer, were included in the experimental program intentionally, because these waves were expected to have more pronounced effect on mixing than waves in the first case.


## 4. Results

The results corresponding to the first series of laboratory experiments conducted for still water conditions are presented in Figures5 and 6. The plots show experimental data of the initial and final temperature distribution over depth, initial temperature applied in the derived diffusion model, and the comparisons between theoretical results and experimental data for the final temperature distribution.Figure 5
(a) Recorded initial and final temperature distribution for still water conditions,t=3600 s. (b) Initial temperature distribution for still water conditions, ∙∙∙ experimental data, — model. (c) Final temperature distribution for still water conditions, ∙∙∙ experimental data, — model.
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(c)Figure 6
(a) Recorded initial and final temperature distribution for still water conditions,t=2700 s. (b) Initial temperature distribution for still water conditions, ∙∙∙ experimental data, — model. (c) Final temperature distribution for still water conditions, ∙∙∙ experimental data, — model.
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(c)The results in Figures5 and 6 show that the temperature in the water column decreases in the upper water layer and increases in its lower part, as expected. The rate of change of the temperature is higher in the upper layer which is related with higher gradients of temperature in this layer. The derived model predicts fairly well the initial and final temperature distribution in the water column. A reasonable agreement between theoretical results and experimental data is observed for both considered cases of initial temperature distributions. The comparisons indicate that the model is applicable even to cases when gradients in temperature distributions over water depth are fairly high.In the second series of laboratory experiments regular wave trains were generated by the wavemaker to study the effect of surface waves on the vertical mixing process. The results are presented in Figures7 and 8. The plots show experimental data of the initial temperature distribution and the final distribution of temperature over depth caused by diffusion process and wave-induced mixing, initial temperature distribution applied in the derived model, and the comparisons between theoretical results and experimental data for the final temperature distribution. The comparisons were conducted for α=0.002 that was assessed based on results corresponding to waves generated in the first case.Figure 7
(a) Recorded initial and final temperature distribution for mixing affected by waves ofL/h=2, t=3600 s. (b) Initial temperature distribution for mixing affected by waves of L/h=2, ∙∙∙ experimental data, — model. (c) Final temperature distribution for mixing affected by waves of L/h=2, ∙∙∙ experimental data, — model.
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(c)Figure 8
(a) Recorded initial and final temperature distribution for mixing affected by waves ofL/h=4, t=3000 s. (b) Initial temperature distribution for mixing affected by waves of L/h=4, ∙∙∙ experimental data, — model. (c) Final temperature distribution for mixing affected by waves of L/h=4, ∙∙∙ experimental data, — model.
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(c)The results in Figures7 and 8 show that the temperature in the water column decreases in the upper water layer and increases in its lower part. The plots show that the rate of change of the temperature is higher in the upper layer than at the lower water levels. The results indicate that waves increase mixing process. The rate of change of the temperature is higher when waves contributed to mixing process and this process increases with increasing the wavelength to water depth ratio. The derived model predicts fairly well the initial and final temperature distribution in the water column. A reasonable agreement between theoretical results and experimental data is observed for both considered cases of initial temperature distributions. The comparisons indicate that the model is applicable even to cases when gradients in temperature distributions over water depth are fairly high.A fairly good agreement obtained between theoretical results and experimental data and the analysis of (14) indicate that for typical ocean waves, which are about two orders of magnitude higher than waves considered in laboratory experiments, the contribution of water waves to mixing may be several orders of magnitude higher than a corresponding contribution arising from a diffusion process. This implies a need to conduct more theoretical studies and experimental investigation on the effect of water waves on mixing processes.


## 5. Summary

Theoretical investigations supported by a series of original laboratory experiments are conducted to study a wave-induced vertical mixing process. An initial boundary-value problem is formulated to describe the evolution of mixing and is solved by applying eigenfunction expansions and a time-stepping procedure. The derived semi-analytical solution is very efficient and is applied to predict the effects of water waves on the temperature changes and the evolution of temperature profiles.The results show that the temperature in the water column decreases in the upper water layer and increases in its lower part, as expected. The rate of change of the temperature is higher in the upper layer, which is related with higher gradients of temperature in this layer. The results indicate that waves increase mixing process. The rate of change of the temperature is higher when waves contributed to mixing process and this process increases with increasing the wavelength to water depth ratio.The analysis indicates that for typical ocean waves the contribution of water waves to mixing may be several orders of magnitude higher than a corresponding contribution arising from a diffusion process. This implies a need to conduct more theoretical studies and experimental investigation on the effect of water waves on mixing processes.A series of original laboratory experiments were conducted in the insulated wave flume to verify the derived model. The comparisons show a reasonable agreement between predicted and measured temperature profiles. A reasonable agreement between theoretical results and experimental data is observed for the whole considered range of initial temperature distributions. The comparisons indicate that the model is applicable even to cases when gradients in temperature distributions over water depth are fairly high.



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*Source: 950849-2015-07-07.xml*