Energy Spectrum of Linear Internal Wave Field in the Vicinity of Continental Slope

The purpose of the research was to investigate two-dimensional modeling of efficiency of mixing, resulting from the reflection of a linear internal wave field (IWF) off a continental slope. Efficiency of deep ocean mixing was associated with the energy balance of the radiating IWF into an interior of the ocean in the vicinity of a sloping bottom topography. Since waves are generated not only at the fundamental frequency but also at all of its harmonics n n ω ω = less than buoyancy frequency N and greater than Coriolis frequency f, our analysis includes, in general, an infinite number of discrete internal wave modes n satisfying the dispersion relationship for internal waves. How-ever, since we are interested only in the radiating part of the field, the mode numbers are limited. Due to multiple singularities of order two caused by resonance in the vicinity of critical slope, the energy is visualized in L δ -norm with 2 δ> . Research results include the visualization of the effects of the continental slope and the Earth’s rotation on resulting energy in the vicinity of the slope.


Introduction
Internal waves occur in density stratified fluids in the presence of a gravitational field. They arise as a result of perturbations which force the stratified fluid to move vertically (i.e. against gravity). Internal wave field (IWF) has periods be-notation f is the inertial frequency, which depends on the rotation rate of the earth (angular velocity Ω ) and the latitude φ : ( ) 2 sin f φ = Ω (1) and N is the (depth-dependent) buoyancy frequency, defined by: ( ) where g is the gravitational acceleration and 0 ρ is the mean density of the medium and The seafloor is one of the critical controls on the ocean's general circulation.
Near bottom topography such as a continental slope, and internal waves, sometimes reaching storm proportions, causes that a strong mixing precesses playing an important role in redistributing sediments and organic matter in deep water, leading to the formation of vast sediment drifts [1] [2] [3] [4]. Mixing efficiency in the ocean due to interaction of IWF near the critical slope of a continental slope makes the IWF generation more effective than that due to supercritical or subcritical slopes [4] [5]. The enhancement of vertical mixing over regions of rough topography has important implications for the abyssal stratification and circulation of the ocean [6] [7] [8].
The subject of mixing processes due to breaking of internal waves in the ocean and atmosphere has received much attention in recent years. In particular, the problem of determining the sources of mechanical energy for mixing in the oceans and atmosphere is an important problem for local micrometeorology [3] [9] [10] [11] [12] and in controlling large-scale ocean circulation [13] [14] [15] [16]. Recent measurements in regions of continental slope characterized by ridges and valleys running up and down the slope by [17] and [18] suggest that 40% -50% of the required energy available for mixing is produced by tide-topography interactions. This has recently been confirmed in our previous analytical studies [14] [ 19], where the process of internal wave generation by the interaction of an oscillatory three-dimensional background flow over a uniform slope has been considered (in the model considered in [19], the upper radiation condition has been used). Observations by Polzin et al. in [20] and [21] suggest that diapycnal mixing is strongly enhanced over rough bottom topography which can be associated with the conversion of barotropic tidal energy into baroclinic tidal energy and the subsequent instability and breaking of internal waves in the ocean.

R. N. Ibragimov et al. Journal of Applied Mathematics and Physics
The length of the world's continental slopes in the oceans sums up to 300,000 km. About 65% of all continental slopes descend in deep sea regions. The rest of the slopes located in the shallow regions of the oceans (see Figure 1). It has been observed that the "Pacific Continental Slope" is steeper than the "Atlantic Continental Slope" whereas the continental slope gradients are flattest in the Indian Ocean [18]. The continental slopes occupy almost 8.8% of the world's surface.
As has been pointed out in [22], increased habitat heterogeneity in canyons is responsible for enhancing benthic biodiversity and creating biomass hotspots. So canyons in the U.S. East Coast were a high priority for federal and state agencies research programs.
The primary focus of this paper is to investigate two-dimensional efficiency of mixing, resulting from the reflection of a linear IWF off a continental slope. The effects of rotation on a linear IWF waves are investigated numerically and using an analytical non-hydrostatic Boussinesq and rigid lid approximations. However, because of the inclusion of high-frequency waves, we cannot make the hydrostatic approximation. Efficiency of deep ocean mixing is associated with the energy balance of the radiating IWF into an interior of the ocean in the vicinity of a sloping bottom topography. Since waves are generated not only at the fundamental frequency but also at all of its harmonics n n ω ω = spanning the range of possible frequencies , our analysis includes, in general, an infinite number of discrete internal wave modes n satisfying the dispersion relationship for internal waves. However, since we are interested only in the radiating part of the IWF, the mode numbers are limited. In order to separate the spectrum irregularities caused by waves of fundamental frequency of mode 1 n = from resonance due to higher harmonic waves ( 1 n > ) in the vicinity of critical slope, the energy is visualized in L δ -norm with 2 δ > .

Two-Dimensional Boussinesq Model and Linearization
In the domain of continuous motion (i.e. in the domain where the velocity , pressure p, density ρ and their first derivatives are continuous), integral conservation laws are equivalent (see e.g. [23]) to the following system of differential equations [6] [24] [25]: which are the momentum balance equation, the continuity equation and conservation of mass.
In Equations (3)-(5), ∇ is the gradient operator and k  denotes a unit vector in the vertical direction. By convention, the xy-plane is tangent to the surface of the ocean with ( ) , , x y z pointing (east, north, up). The term 2 × v  Ω is referred to as the Coriolis acceleration. Note that the momentum balance Equation In most geophysical systems, the fluid density varies, but not greatly, around a mean value (more specifically, the density variations in the ocean do not exceed 3% -4%). This observation is the basis for the Boussinesq approximation, which replaces the exact density by a constant representative value in many terms of the equations of motion (see also [25]).
Without approximation, we may divide the exact ocean density into a con- Thus, to a very good approximation, where D t The approximation (6) is called the Boussinesq approximation [25].
In summary, the Boussinesq approximation, rooted on the assumption that the density does not depart much from a mean value, has allowed us to replace the exact density ρ by its reference value 0 ρ everywhere, except in front of the gravitational acceleration and in the energy equation, which has become an equation governing density variations.
In two dimensions, the incompressibility condition is taken into account by introducing a stream function ψ which is related to the two velocity components u and w by , where the nonlinear advective terms are written by means of the Jacobian oper- and subscripts denote partial differentiation. We look for solutions where ε characterizes the size of the perturbation due to the waves. We then have ( ) In the linear approximation, obtained by setting 0 ε = , we can derive a single equation for 1 ψ which we will call ψ , where A is a constant and ϕ is the phase constant. Substitution of representation (15) into (14) leads to the dispersion relation of internal waves where k and m are wavenumbers of the wave vector . Dispersion relation (16) relates the frequency ω to the parameters , , N f k and m. Unlike for surface waves, the wave vector of internal plane waves is perpendicular to the group velocity and, thus, to the direction of the energy propagation. Hereafter it is assumed that N is a constant value, which is set to be 10 −3 s −1 . As follows from the relation (16), the range of possible frequencies is limited, This means that internal waves with frequencies greater than buoyancy frequency or with frequencies less than inertial frequency cannot exist. Internal waves of inertial frequency are horizontal rotations of water parcels; internal waves at the buoyancy frequency (when m/k is small, N ω ≈ and, hence, rotation effects are negligible) are purely vertical oscillations of water parcels. In both these limiting cases the group velocity is zero and there is no wave propagation. At intermediate frequencies, the parcels move in oblique elliptical orbits.
It is worth noting that f goes to zero as the equator is approached and therefore the rotational effect becomes smaller and this has an important effect on the internal wave structure and dynamics.

Vertical Modes and Rigid Lid Approximation
With the boundary conditions, appropriate for a flat bottom at 0 z = and rigid lid at z H = , where H is the (range-independent) depth of the water column, we can look for a separable so- To a good approximation, a rigid lid approximation holds for IWF which produces very small vertical displacement at the free surface. Because of the small density variations ( Solving this equation using the boundary conditions (18) (20) can be expressed as a linear combination of these modes: Equation (20) can also be used to obtain solutions for a wave propagating horizontally with a large enough wavelength to feel a bottom.
When the boundary conditions (18) are used one can readily verify that is a solution of (20) and thus there exist an infinite number of discrete internal wave modes satisfying the relationship (16), i.e.
Thus in our model (14) we can set where A is an amplitude of the isopycnal displacement and ϕ is a constant phase.
Since N is assumed to be a constant and the coefficients of Equation (14) are independent of spatial variables, we can superimpose solutions of the form (24) to get more general solutions to the ( )

Energy of IWF
To get the formula expressing the total energy of a IWF, we find it useful to re-Journal of Applied Mathematics and Physics write the linearized governing equations combining the Boussinesq approximation (6) in the component form, i.e.
Following [24] we obtain the energy equation of linear internal waves by multiplying (28) by u, (29) by v, (30) From (33) we define the averaged linear energy density E by ( ) where an overbar is used to define the mean over a wavelength. Substituting solutions (25)- (27) into (34) we obtain the averaged linear energy density for each wave in the form where i is the wave number in our model.

Reflection of Waves
We approximate a continental slope by a uniform slope z Since the normal velocity vanishes on the slope, the boundary condition is where the subscript R is used to denote the component of the reflected wave.
Since the frequencies of the incident and reflected waves must be the same,

Visualization of IWF Reflected Wave off the Slope
We study the IWF reflected wave off the slope if the incident wave field is known.
The energy (36) of each wave is calculated as follows: First, according to (22) Finally, we find i k from the dispersion relation (23) as follows: ; , where i R is the discrete number of waves in the frequency band i.

Fundamental Frequency (n = 1)
First, we visualize the dominant contribution to energy density (53) of IWF as a function of frequency when 1 n = . In this case, since higher harmonic waves don't contribute, we set 1 δ = . Figure 3 Figure 4 shows the energy density for two cases: 1) subcritical slopes We can can also observe that the energy is a monotonically increasing function of frequency for subcritical values of a continental slope α and the energy has singularities for supercritical values of a continental slope α .

Harmonic Frequency (n ≥ 1)
The contribution of higher harmonic waves into energetics of the reflected IWF off a slope is analyzed with 3 δ = and visualized in Figure 5.     Overall, the energy density of fundamental frequency 1 n = increases with α , reaching a maximum at ( ) 0 α * , the cutoff frequency for the lowest harmonic.
It then drops significantly, due to the loss of waves of the fundamental frequency, and then increases as α continues to increase reaching a second maximum (singular frequency) at which point it drops again as waves of second harmonic frequency are lost. The process continues until all the harmonics are lost.
As an additional; illustration to our modeling, the total energy density in ( ) , n ω and in ( ) , k n -spaces is shown in Figure 8 and Figure 9. We can see that the most energetic part of the spectrum is contained at lower mode numbers and frequencies of ( ) , n ω -space. Namely, the effects of increasing slope, both approaching and exceeding the critical angle, can be observed in Figure 8 in the harmonic case. After the slope exceeds the critical angle, a large spike in energy occurs at lower mode numbers and frequencies.
Thus the effects of increasing slope, both approaching and exceeding the critical angle, can be observed in Figure 8 in the harmonic case. After the slope exceeds the critical angle, a large spike in energy occurs at lower mode numbers frequencies.
Similarly, Figure 9 shows the log of energy distribution in ( ) We can see that the most energetic part of the spectrum is contained at the higher horizontal wavenumber-higher mode number region of ( ) , k n -space.

Conclusions
The results of studies in [16] [17] [18] and [20] show that the ocean mixing is most efficient near bottom irregularities. One particular region of ocean mixing occurs near Mid-Atlantic Ridge (see e.g. [18] or [28]). Our recent numerical results and analytical studies in [19] of internal tide generation over a continental slope confirm the results in [29], showing that the turbulent dissipation is in-Journal of Applied Mathematics and Physics creased due to nonlinear effects and mixing near Mid-Atlantic Ridge. The problem of reflection of internal waves from a plane boundary in different contexts was studied in [27] [28] and [30] [31] [32]. Recent laboratory observations of reflected internal waves on sloping boundaries at a moderately large Reynolds number were reported in [33]. The particular question of reflecting internal wave beams was studied in [34] and [35].
We have developed the numerical algorithm designed to analyze the effects of rotation on the energy distribution of linear IWF in the vicinity of the critical slope. Since waves are generated not only at the fundamental frequency but also at all of its harmonics n n ω ω = spanning the range of possible frequencies , our analysis includes, in general, an infinite number of discrete internal wave modes n satisfying the dispersion relationship for internal waves.
Our algorithm allows to analyze separately the contribution of fundamental frequency and higher harmonic waves on the linear energy distribution. Higher harmonic waves contribute to multiple singularities of the function G defined by (54). So we have introduced the L β -norm in order to smooth out the spectral irregularities of the reflected IWF spectrum.
To conclude, our numerical algorithm gave us insight into the effects of continental slope and latitude on energy of a linear reflected internal wave field. In this model, our bathymetry is given by a simple slope, which is used to approximate continental slope. Also, the developed algorithm could be used to expand the existing model to incorporate small amplitude, gentle slope bell-shape topography, which would yield a model much more representative of the ocean floor, and therefore the internal wave fields contributing to mixing in the ocean. This analysis will be reported in the forthcoming studies published elsewhere.