Linear Boltzmann Model for Wave Scattering in the MIZ

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We present a linear Boltzmann equation to model Wave Scattering in the Marginal Ice Zone. This model is three dimensional and requires the three-dimensionao solution for a Floating Elastic Plate. This model was given in Meylan and Masson 2006 (which also showed the equivalence with The Multiple Scattering Theory of Masson and LeBlond). The derivation closely follows that of Meylan, Squire, and Fox 1997 with a correction.

The wave scattering which occurs in the MIZ is due to the scattering effects of the individual ice floes which comprise the MIZ. To understand the process of wave scattering we need to understand the scattering which any individual ice floe produces. However, the equation for the propagation of wave energy, while dependent on the scattering from individual floes, will take a form quite different to the equation of scattering from an individual floe.

Determining the scattering at the large scale from the scattering from an individual scatterer is important in many areas of physics. There are many approaches to this problem, the two most popular being the linear Boltzmann (or transport) equation, and multiple scattering. However, the MIZ presents a slightly more complex case than is usually encountered in scattering theories because of the random nature of the scatterers (i.e. the random geometry of ice floes) and the constant motion of the ice floes. This means that it is extremely unlikely that any kind of coherent scattering effects will be observed. However, all large scale scattering theories require as input the individual scatterers and often assume that all scatterers are identical. This can lead, in the scattering theory, to coherent scattering effects which we believe are not significant for the MIZ.

The Linear Boltzmann equation for Wave Scattering in the MIZ

In this section we present a derivation of the linear Boltzmann equation for wave scattering in the MIZ that follows closely the derivation given in Meylan, Squire, and Fox 1997 but corrects an error in this earlier derivation. The linear Boltzmann equation is applicable to the propagation of wave energy through the MIZ over length and time scales large relative to the incident wavelength and wave period, respectively. Over such large scales, we assume that wave energy is incoherent. We consider the surface of an infinitely deep ocean represented in Cartesian co-ordinates by [math]r =(x,y).[/math] Wave energy is propagating across this surface in all directions so that, at any point, we must consider the energy travelling in each direction. We introduce an intensity function [math]I(r,t,\theta)[/math] which is the rate of flow of energy travelling in a given direction, per unit surface, per unit angle. In the absence of scatterers, we assume that the waves continue to propagate in the same direction and that the energy intensity satisfies the following equation,

[math] \frac{1}{c_{g}}\frac{\partial}{\partial t}I(r,t,\theta)+\hat{\theta}.\nabla I(r,t,\theta)=0,\,\,\,(1) [/math]

where [math]\hat{\theta}[/math] is a unit vector in the [math]\theta[/math] direction and [math]c_{g}[/math] is the speed of wave propagation (the deep water group speed). The presence of the floes will modify this expression by scattering energy, i.e. by changing the direction in which the energy is travelling.

We modify equation (1) to take into account the scattering effects of the ice floes using the general equation for the propagation of wave energy through a scattering medium,

[math] \frac{1}{c_{g}}\frac{\partial}{\partial t}I(r,t,\theta)+\hat{\theta}.\nabla I(r,t,\theta)=-\beta(r,\theta)I(r,t,\theta)+\int_{0}^{2\pi}S(r,\theta,\theta ^{\prime})I(r,t,\theta^{\prime})d\theta^{\prime},\,\,\,(2) [/math]

(Howells 1960) where [math]\beta[/math] is the absorption coefficient and [math]S[/math] is the scattering function (assumed to be independent of time). Equation (2) depends on the assumption that each floe scatters independently and that the energy from different scatterers may be added incoherently. The absorption coefficient, [math]\beta(r,\theta)[/math], is the fraction of energy lost by scattering and dissipative processes (assumed linear) from a pencil of radiation in direction [math]\theta[/math], per unit path length travelled in the medium. The scattering function [math]S(r,\theta,\theta^{\prime })[/math] specifies the angular distribution of scattered energy in such a way that,

[math] S(r,\theta,\theta^{\prime})I(r,t,\theta^{\prime})d\Omega dSd\Omega^{\prime},,\,\,\,(3) [/math]

is the rate at which energy is scattered from a pencil of radiation of intensity [math]I(r,t,\theta^{\prime})[/math] at an angle [math]d\Omega^{\prime} [/math] in direction [math]\theta^{\prime}[/math], by a surface [math]dS[/math] at position [math]r[/math], into an angle [math]d\Omega[/math] in direction [math]\theta[/math]. To apply equation (2) to wave scattering in the MIZ we must first estimate the scattering function [math]S(r,\theta,\theta^{\prime})[/math] and the absorption coefficient [math]\beta(r,\theta)\,[/math].

Finding the scattering and absorbtion functions

The scattering function is determined by calculating the scattering from a single ice floe. Each ice floe scatters energy, and the energy radiated per unit angle per unit time in the [math]\theta[/math] direction for a wave incident in the [math]\theta^{\prime}[/math] direction, [math]E[/math], is given by,

[math] E(\theta - \theta^{\prime})=\left( \frac{H}{2}\right) ^{2}\frac{\rho\omega g}{4k}|D(\theta-\theta^{\prime})|^{2},\,\,\,(4) [/math]

where [math]H[/math] is the wave height, [math]\rho[/math] is the water density, [math]\omega[/math] and [math]k[/math] are the radian frequency and wavenumber of the wave, respectively, and [math]g[/math] is the acceleration due to gravity. [math]D(\theta - \theta^{\prime})[/math] is the scattered amplitude for which, at a large distance, [math]r[/math], from the scatterer, the asymptotic amplitude of the outgoing wave in the [math]\theta[/math] direction, for an incident wave travelling in the [math]\theta^{\prime}[/math] direction, is given by

[math] \frac{H}{2}\frac{D\left( \theta - \theta^{\prime}\right) }{\sqrt{r}},\,\,\,(5) [/math]

Note that, in equations (4) and (5), we have assumed that the scattering is isotropic (depends only on the difference of angle). This will not necessarily be true for a given ice floe, but we expect this to be true in the MIZ since there are no special directions in which the ice floes are oriented, and the floes are of random shape.

We must now express the scattering kernel in equation (2), [math]S(r,\theta,\theta^{\prime})[/math], in terms of [math]E[/math]. Given the definition of [math]S[/math] (equation (\ref{equation_S})), [math]S[/math] can be found by dividing [math]E[/math] by the rate of energy which is passing under the ice floe. The rate of energy passing under the floe is given by the product of the wave energy density ([math]\frac{1}{8}\rho gH^{2},[/math] since [math]H/2[/math] is the wave amplitude and we are considering only the energy in the water), the average area occupied by a floe ([math]A_{f}/f_{i},[/math] where [math]A_{f}[/math] is the average area of the floe and [math]f_{i}[/math] is the fraction of the surface area of the ice covered ocean which is covered in ice), and the wave group speed ([math]\omega/2k)[/math]. This gives the following expression for [math]S[/math],

[math] S(\theta,\theta^{\prime}) =\left( \frac{H}{2}\right) ^{2}\frac{\rho\omega g}{4k}|D(\theta-\theta^{\prime})|^{2}\frac{4f_{i}k}{\rho gH^{2}A_{f}\omega} =\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime})|^{2},\,\,\,(6) [/math]

This expression is not exactly the same as the equivalent expression in Meylan, Squire, and Fox 1997 because, in the derivation for [math]S[/math] in Meylan, Squire, and Fox 1997, the wave phase speed rather than the group speed was erroneously used.

We can determine [math]\beta[/math] from the absorption cross section, [math]\sigma_a[/math], and the ice cover fraction [math]f_i[/math] he absorption cross section, [math]\sigma_a[/math], may be estimated from the total scattering or from experimental measurements. The expression for [math]\beta[/math] is the following,

[math] \beta = \int_{0}^{2\pi}\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime})|^{2}d\theta^{\prime}+\sigma_{a} \frac{f_{i}}{A_{f}},\,\,\,(7) [/math]

Combining equations (2), (6) and (7), the following linear Boltzmann equation for wave scattering in the MIZ is obtained,

[math] \frac{1}{c_g}\frac{\partial I}{\partial t}+\hat{\theta}.\nabla I = \int_{0}^{2\pi}\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime })|^{2}I\left( \theta^{\prime}\right) d\theta^{\prime} - \left( \int_{0}^{2\pi}\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime})|^{2}d\theta^{\prime}+\sigma_{a} \frac{f_{i}}{A_{f}} \right)I\left( \theta\right),\,\,\,(8) [/math]

Determining the scattering amplitude

We need to determine the scattering amplitude [math]D(\theta-\theta^{\prime})[/math]. The scattering amplitude is found by solving the boundary value problem which arises when an isolated floe is subject to linear wave forcing. The exact equations depend on the equations chosen to model the movement of the ice floe. The solution to the equations of motion depends on the model used to describe an ice floe. The principal difference between the ice floe models used by Meylan, Squire, and Fox 1997 and Masson and LeBlond 1989 is the following. Meylan, Squire, and Fox 1997 assumed that the ice floe was a Floating Elastic Plate while Masson and LeBlond 1989 assumed the floes were rigid but allowed for submergence. Both models have different ranges of validity (although typical ice floes tend to be relatively thin). Of course, either ice floe model could have been used in the large scale scattering models derived by Masson and LeBlond 1989 and Meylan, Squire, and Fox 1997. Here we simply present the equation for [math]D(\theta)[/math] independent of the equation used to model the ice floe.

The linearised boundary value problem for the fluid velocity potential [math]\phi({r},z)[/math] subject to an incoming wave of frequency [math]\omega[/math] is the Standard Linear Wave Scattering Problem in infinitely deep water which we briefly recap here.

[math] \nabla^{2}\phi=0, \, -\infty\ltz\lt0,\,\,\,(9) [/math]

[math] \frac{\partial\phi}{\partial z}=0, \, z\to-\infty, [/math]

[math] \frac{\partial\phi}{\partial z} = k\phi,\,z\in\Gamma_s, [/math]

[math] \frac{\partial\phi}{\partial z} = L\phi, \, z\in\Gamma_w, [/math]

(note that since the water is assumed infinitely deep [math]k_\infty = k[/math]). The free surface is [math]\Gamma_s[/math] (located at [math]z=0[/math]) and the wetted surface of the ice floe is [math]\Gamma_w[/math]. At the wetted surface of the ice floe the exact equation of motion depends on the way in which the floe is modelled (for example whether it is flexible or rigid) and we represent this by the operator [math]L[/math]. To actually solve equation (9) requires us to choose a specific model for the ice floe and hence to determine [math]L[/math].

Equation (9) requires boundary conditions as [math]x[/math] or [math]y[/math] tend to infinity which are found from the incident or driving wave, denoted [math]\phi^{\mathrm{{In}}}[/math] which we assume is a plane wave travelling in the [math]x[/math] direction,

[math] \phi^{\mathrm{{In}}}({ r},z)=\frac{\omega}{k}e^{{\rm i}kx}e^{kz}. [/math]

plus the Sommerfeld Radiation Condition.

Once we have found the solution to equation (9), we obtain the absolute value of the scattering amplitude [math]D[/math] as

[math] \left\vert D\left( \theta\right) \right\vert =\left( \frac {k}{2\pi}\right) ^{1/2}\left( \frac{\omega}{g}\right) \left\vert \mathbf{H}\left( \pi+\theta\right)\right\vert, [/math]

where the Kochin Function [math]\mathbf{H}(\tau)[/math] is

[math] \mathbf{H}(\tau)=\iint_{\Gamma_s}\left( -\frac{\delta\phi}{\delta n} + \phi\frac{\delta}{\delta n}\right) e^{kz}e^{ik(x\cos\tau +y\sin\tau)}dS, [/math] where [math]\delta/\delta n[/math] is the inward normal derivative.

Numerical Solution of the Transport Equation

We present here a simple method to solve the linear Boltzmann equation. It involves simplifying assumptions of the spatial or temporal independence of the solution as well as a discretisation of the equation in angle. We begin by assuming that the solution is only a function of the [math]x[/math] spatial co-ordinate and time, i.e. there is no [math]y[/math] dependence of the solution. We also consider a uniform MIZ so that the scattering function, [math]S[/math], is a function only of [math]\theta[/math] and [math]\theta^{\prime}[/math] and [math]\beta[/math] is a constant. The only variation we allow spatially is that the MIZ occupies the region [math]x\gtb[/math], i.e. the ice edge is at [math]x=b.[/math] This will allow us to consider a wave spectrum which enters the MIZ from the open ocean. Under these assumptions equation (8) becomes,

[math] \frac{1}{c_{g}}\frac{\partial I}{\partial t}+\cos\theta\frac{\partial I}{\partial x}=\left\{ \begin{bmatrix} -\beta I+\int_{0}^{2\pi}S(\theta-\theta^{\prime})I(\theta^{\prime} )d\theta^{\prime},\;\;x\gtb, \\ 0,\;\;x\ltb. \end{bmatrix} \right.\,\,\,(10) [/math]

To solve equation (10) we convert the problem to a matrix equation by introducing a discretisation in angle. We use a discrete ordinate method (\cite{Case&Zweifel}) and represent the angular coordinate by a discrete set of [math]n[/math] angles evenly spaced between [math]0[/math] and [math]2\pi[/math] ([math]\theta_{j}=\frac{2\pi j}{n},\;0\leq j\leq n-1,[/math]). This approximation converts equation (10) to the following equation,

[math] \frac{1}{c_{g}}\frac{\partial\vec{I}}{\partial t}-\frac{\partial}{\partial x}\mathbf{{D}}\vec{I}=\mathbf{\left\{ \begin{bmatrix} -\beta \vec{I}+\mathbf{S}\vec{I},\;\;x\gtb,\\ 0,\;\;x\ltb. \end{bmatrix} \right. }\,\,\,(11) [/math]

In equation (11) the intensity [math]\vec{I}[/math] is now a vector of functions of [math]x[/math] and </math>t</math> for each angle [math]\theta_{j}[/math] and the elements of the matrices [math]\mathbf{{D}}[/math] and [math]\mathbf{{S}}[/math] are given by,

[math] d_{ij}=\left\{ \begin{bmatrix} -\cos(\theta_{i}), & i=j,\\ {0,} & i\neq j, \end{bmatrix} \right. [/math]


[math] s_{ij}=\left\{ \begin{bmatrix} {-}\beta{+}S(\theta_{i}-\theta_{i})\frac{2\pi}{n}{,} & i=j,\\ S(\theta_{i}-\theta_{j})\frac{2\pi}{n}{,} & i\neq j, \end{bmatrix} \right. [/math]

respectively. Equation (11) can be easily solved in the stationary (no time dependence), or isotropic (no spatial dependence) case. Meylan, Squire, and Fox 1997 solved the stationary problem and Masson and LeBlond 1989 solved the isotopic problem (with wind forcing etc.). In the stationary case equation (11) reduces to, setting the ice edge to [math]b=0,[/math]

[math] -\frac{\partial}{\partial x}\mathbf{D}\vec{I}=-\beta\vec{I}+\mathbf{S}\vec{I}, \;\;x\gt0.\,\,\,(12) [/math]

For the isotropic case, equation (\ref{matrix}) reduces to, setting the ice edge to [math]b=-\infty[/math],

[math] \frac{1}{c_{g}}\frac{\partial}{\partial t}\vec{I}=-\beta\vec{I}+\mathbf{S} \vec{I},\;\;t\gt0.\,\,\,(13) [/math]

Equations (12) and (13) can be solved by straightforward matrix methods. Equation (12) requires boundary conditions (the wave spectrum at the ice edge [math]x=0[/math] and a condition as [math]x\to\infty[/math]) and equation (13) requires an initial condition (the wave spectrum at [math]t=0[/math]).