# Introduction

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 The equation is derived by two methods, the first based on Masson and LeBlond 1989 and the second based on Meylan, Squire and Fox 1997.

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 the multiple scattering,

both described in \cite{ishimaru}. 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 \cite{jgrrealism} 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 ${\bf r} =(x,y).$ 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 $I({\bf r},t,\theta)$ 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, $$\label{no_scattering} \frac{1}{c_{g}}\frac{\partial}{\partial t}I({\bf r},t,\theta)+\hat{\theta}.\nabla I({\bf r},t,\theta)=0,$$ (\cite{phillips77}) where $\hat{\theta}$ is a unit vector in the $\theta$ direction and $c_{g}$ 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 (\ref{no_scattering}) 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, $$\frac{1}{c_{g}}\frac{\partial}{\partial t}I({\bf r},t,\theta)+\hat{\theta}.\nabla I({\bf r},t,\theta)=-\beta({\bf r},\theta)I({\bf r},t,\theta)+\int_{0}^{2\pi}S({\bf r},\theta,\theta ^{\prime})I({\bf r},t,\theta^{\prime})d\theta^{\prime}, \label{Howells}%$$ (\cite{howells60}) where $\beta$ is the absorption coefficient and $S$ is the scattering function (assumed to be independent of time). Equation~(\ref{Howells}) depends on the assumption that each floe scatters independently and that the energy from different scatterers may be added incoherently. The absorption coefficient, $\beta({\bf r},\theta)$, is the fraction of energy lost by scattering and dissipative processes (assumed linear) from a pencil of radiation in direction $\theta$, per unit path length travelled in the medium. The scattering function $S({\bf r},\theta,\theta^{\prime })$ specifies the angular distribution of scattered energy in such a way that, $$\label{equation_S} S({\bf r},\theta,\theta^{\prime})I({\bf r},t,\theta^{\prime})d\Omega dSd\Omega ^{\prime},$$ is the rate at which energy is scattered from a pencil of radiation of intensity $I({\bf r},t,\theta^{\prime})$ at an angle $d\Omega^{\prime}$ in direction $\theta^{\prime}$, by a surface $dS$ at position ${\bf r}$, into an angle $d\Omega$ in direction $\theta$. To apply equation (\ref{Howells}) to wave scattering in the MIZ we must first estimate the scattering function $S({\bf r},\theta,\theta^{\prime})$ and the absorption coefficient $\beta({\bf r},\theta)$.

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 $\theta$ direction for a wave incident in the $\theta^{\prime}$ direction, $E$, is given by, $$E(\theta - \theta^{\prime})=\left( \frac{H}{2}\right) ^{2}\frac{\rho\omega g}{4k}|D(\theta-\theta^{\prime})|^{2},\label{energyrad}%$$ where $H$ is the wave height, $\rho$ is the water density, $\omega$ and $k$ are the radian frequency and wavenumber of the wave, respectively, and $g$ is the acceleration due to gravity. $D(\theta - \theta^{\prime})$ is the scattered amplitude for which, at a large distance, $r$, from the scatterer,

the asymptotic amplitude of the


outgoing wave in the $\theta$ direction, for an incident wave travelling in the $\theta^{\prime}$ direction, is given by $$\label{energyrad_D} \frac{H}{2}\frac{D\left( \theta - \theta^{\prime}\right) }{\sqrt{r}}.$$ Note that, in equations~(\ref{energyrad}) and (\ref{energyrad_D}), 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 (\ref{Howells}), $S({\bf r},\theta,\theta^{\prime})$, in terms of $E$. Given the definition of $S$ (equation (\ref{equation_S})),

$S$ can be found by


dividing $E$ 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 ($\frac{1}{8}\rho gH^{2},$ since $H/2$ is the wave amplitude and we are considering only the energy in the water), the average area occupied by a floe ($A_{f}/f_{i},$ where $A_{f}$ is the average area of the floe and $f_{i}$ is the fraction of the surface area of the ice covered ocean which is covered in ice), and the wave group speed ($\omega/2k)$. This gives the following expression for $S$, \begin{align} 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} \nonumber \label{scatteringfromeng2}\\ & =\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime})|^{2}. \end{align} This expression is not exactly the same as the equivalent expression in \cite{jgrrealism} because, in the derivation for $S$ in \cite{jgrrealism}, the wave phase speed rather than the group speed was erroneously used.

We can determine $\beta$ from the absorption cross section, $\sigma_a$, and the ice cover fraction $f_i$ (M\&Le p. 58). The absorption cross section, $\sigma_a$, may be estimated from the total scattering or from experimental measurements. The expression for $\beta$ is the following, $$\label{beta_equation} \beta = \int_{0}^{2\pi}\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime})|^{2}d\theta^{\prime}+\sigma_{a} \frac{f_{i}}{A_{f}}.$$

Combining equations (\ref{Howells}), (\ref{scatteringfromeng2})\ and (\ref{beta_equation}),

the following linear Boltzmann equation for


wave scattering in the MIZ is obtained, $$\label{boltzmann} \frac{1}{c_g}\frac{\partial I}{\partial t}+\hat{\theta}.\nabla I = \int_{0}^{2\pi}\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime })|^{2}I\left( \theta^{\prime}\right) d\theta^{\prime} - \left( \int_{0}^{2\pi}\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime})|^{2}d\theta^{\prime}+\sigma_{a} \frac{f_{i}}{A_{f}} \right)I\left( \theta\right).$$

\section{The Multiple Scattering Theory of M\&Le}

The scattering theory of M\&Le was the first model which properly accounted for the three dimensional scattering which occurs in the MIZ. The model was derived using multiple scattering and was presented in terms of a time step discretisation and only for ice floes with a circular geometry. Their scattering theory included the effects of wind generation, nonlinear coupling in frequency and wave breaking. However, what was original in their work was their equation for the scattering of wave energy by ice floes. M\&Le began with the following equation for the evolution of wave scattering, \frac{\partial I}{\partial t}+c_{g}\hat{\theta}.\nabla I= \left( S_{\mathrmTemplate:In% }+S_{\mathrmTemplate:Ds}\right) \left( 1-f_{i}\right) +S_{\mathrmTemplate:Nl% }+S_{\mathrmTemplate:Ice}, \label{BoltzMasson}% where $S_{\mathrmTemplate:In}$ is the input of wave energy due to wind forcing, $S_{\mathrmTemplate:Ds}$ is the dissipation of wave energy due to wave breaking, $S_{\mathrmTemplate:Nl}$ is the non-linear transfer of wave energy and $S_{\mathrmTemplate:Ice}$ is the wave scattering. Similarly, the terms $S_{\mathrmTemplate:In},$ $S_{\mathrmTemplate:Ds},$ and $S_{\mathrmTemplate:Nl}$ could be added to equation (\ref{Howells}). However, the purpose of this paper is to derive a consistent equation for $S_{\mathrmTemplate:Ice}.$ M\&Le

solved equation (\ref{BoltzMasson}) in the isotropic (no spatial


dependence) case. Furthermore, they did not actually determine $S_{\mathrmTemplate:Ice}$ but derived a time stepping procedure to solve the isotropic solution using multiple scattering. We will derive $S_{\mathrmTemplate:Ice}$ from their time stepping equation.

M\&Le derived the following difference equation as a discrete analogue of equation~(\ref{BoltzMasson}) I(f_{n},\theta;t+\Delta t)=[\mathbf{T}]_{f_{n}}[I(f_{n},\theta

t)+((S_{\mathrm{in}}+S_{\mathrm{ds}})(1-f_{i})+S_{\mathrm{nl}})\Delta

t],\label{timestep}% where $f_{n}$ is the wave frequency (M\&Le, equation~(51)). It is important to realise that $[\mathbf{T}]_{f_{n}}$ is a function of $\Delta t$ in the above equation. We are interested only in the wave scattering term so we will set the terms due to wind input ($S_{\mathrmTemplate:In}$), wave breaking ($S_{\mathrmTemplate:Ds}$) and non-linear coupling ($S_{\mathrmTemplate:Nl}$) to zero. These terms can be readily included in any model if required. M\&Le discretized the angle $\theta$ into $n$ evenly spaced angles $\theta_{i}$ between $-\pi$ and $\pi$. $[\mathbf{T}]_{f_{n}}$ is then given by $$(T_{ij})_{f_{n}}=A^{2}\{\hat{\beta}|D(\theta_{ij})|^{2}\Delta \theta+\delta(\theta_{ij})(1+|\alpha_{c}D(0)|^{2}% )+\delta(\pi-\theta_{ij})|\alpha_{c}D(\pi)|^{2} \},\label{wrong}%$$ where $\theta_{ij}=|(\theta_{i}-\theta_{j})|$ (M\&Le, equation~(42)). In equation~(\ref{wrong}), $\hat{\beta}$ (this notation is chosen to follow from M\&Le who used $\beta$ and to avoid confusion with the expression for $\beta$ in equation (\ref{Howells}) and which is used in \cite{howells60} and \cite{jgrrealism}) is a function of $\Delta t$ given by $$\hat{\beta}=\int_{0}^{c_{g}\Delta t}\rho_{e}(r)dr,$$ (M\&Le p. 68). The function $\rho_{e}(r)$ gives the effective number of floes per unit area effectively radiating waves under the single scattering approximation

which is to assume that the amplitude of a wave scattered


more than once is negligible. It is given by \label{rho_e} \rho_{e}(r)=\frac{2}{\sqrt{3}D_{\mathrmTemplate:Av}^{2}\left( 1-\frac{8a^{2}}{\sqrt {3}D_{\mathrmTemplate:Av}^{2}}\right) ^{1/2}}\left( 1-\frac{8a^{2}}{\sqrt {3}D_{\mathrmTemplate:Av}^{2}}\right) ^{r/2a}, (M\&Le equation~(29), although there is a typographical error in their equation which we have corrected) where $D_{av}$ is the average floe spacing and $a$ is the floe radius (remembering that M\&Le considered circular floes). The energy factor $A$ is given by, $$A=(1+|\alpha_{c}D(0)|^{2}+|\alpha_{c}D(\pi)|^{2}+\hat{\beta}\int_{0}^{2\pi }|D(\theta)|^{2}d\theta+f_{d})^{-\frac{1}{2}}\label{equation_A},$$ (M\&Le equation~(52)) where the term $f_{d}$ represents dissipation and is given by $f_{d}=e^{\frac{f_{i}}{A_{f}}\sigma_{a}c_{g}\Delta t}-1,$ (M\&Le equation~(53)) and $\alpha_{c}$, the coherent scattering coefficient, is given by \alpha_{c}=\left( \frac{2\pi}{k}\right) ^{1/2}\exp\left( \frac {\mathrm{{i}\pi}}{4}\right) \frac{2}{\sqrt{3}D_{\mathrmTemplate:Av}^{2}\left( 1-\frac{8a^{2}}{\sqrt{3}D_{\mathrmTemplate:Av}^{2}}\right) ^{1/2}}\int_{0}^{c_g\Delta t }\exp(\mathrmTemplate:Ikx_{s})\left( 1-\frac{8a^{2}}{\sqrt{3}D_Template:Av^{2}}\right) ^{x_{s}/2a}dx_{s}. It should be noted that the upper limit of integration for $\alpha_{c}$ was given as infinity in M\&Le. This is appropriate in the steady case only; it should have been changed to $c_{g}\Delta t$ in the time dependent case. However, this correction leads to only negligible quantitative changes to the results.

We will transform the M\&Le scattering operator $\mathbf{T}$ by taking the limit as the number of angles used to discretise $\theta$ tends to infinity. On taking this limit, the operator $\mathbf{T}\left( \Delta t\right)$ becomes $\mathbf{T}\left( \Delta t\right) I\left( \theta\right) =A^{2}\{\hat{\beta }\int_{0}^{2\pi}|D(\theta-\theta^{\prime})|^{2}I\left( \theta^{\prime }\right) d\theta^{\prime}+ I\left( \theta\right) \}.$

The scattering theory of M\&Le depends on the values of the time step $\Delta t$ and the correct solution is found for small time steps. We will now find the equation in the limit of small time steps by taking the limit as $\Delta t$ tends to zero. As we shall see, when this limit is taken, there is a considerable simplification in the form of the equation. Since $I(t+\Delta t)=\mathbf{T}\left( \Delta t\right) I\mathbf{(}t),$ we obtain the following expression for the time derivative of $I$, $\frac{\partial I}{\partial t}=\lim_{\Delta t\rightarrow0}\left( \frac{\mathbf{T}\left( \Delta t\right)I(t) - I(t)}{\Delta t}\right).$ We can calculate this limit as follows, $\lim_{\Delta t\rightarrow0}\left( \frac{\mathbf{T}\left( \Delta t\right)I(t) -I(t)}{\Delta t}\right) =\lim_{\Delta t\rightarrow0}\left( \frac {A^{2}\{\hat{\beta}\int_{0}^{2\pi}|D(\theta-\theta^{\prime})|^{2}I\left( \theta^{\prime}\right) d\theta^{\prime}+I\left( \theta\right) \}-I\left( \theta\right) }{\Delta t}\right)$

$$\label{M_Le_boltzmann1} =c_{g}\rho_{e}\left( 0\right) \int _{0}^{2\pi}|D(\theta-\theta^{\prime})|^{2}I\left( \theta^{\prime}\right) d\theta^{\prime}-c_{g}\rho_{e}\left( 0\right) \int_{0}^{2\pi}% |D(\theta-\theta^{\prime})|^{2}d\theta^{\prime}+\frac{f_{i}}{A_{f}}\sigma_{a}c_{g}I\left( \theta\right).$$ We can simplify equation~(\ref{M_Le_boltzmann1}) by using equation~(\ref{rho_e}). The value of $\rho_{e}\left( 0\right)$ is given by \label{rho} \rho_{e}\left( 0\right) =\frac{2}{\sqrt{3}D_{\mathrmTemplate:Av}^{2}\left( 1-\frac{8a^{2}}{\sqrt{3}D_{\mathrmTemplate:Av}^{2}}\right) ^{1/2}} =\frac{f_{i}}{A_{f}\sqrt{1-4f_{i}/\pi}}, where we have used the fact that $f_{i}=2\pi a^{2}/\sqrt{3}D_{av}^{2}$ and $A_{f}=\pi a^{2}$.

If we substitute our expressions for $\rho_e(0)$ in equation (\ref{M_Le_boltzmann1}) and include the spatial term (which was not in M\&Le since they assumed

isotropy) and divide by $c_g$, we obtain the following


linear Boltzmann equation \begin{align}\label{M_Le_boltzmann2} \frac{1}{c_g}\frac{\partial I}{\partial t}+\hat{\theta}.\nabla I &=\frac{1}{\sqrt{1-4f_{i}/\pi}} \int_{0}^{2\pi}\frac{f_{i}}{A_{f}}|D(\theta-\theta^{\prime })|^{2}I\left( \theta^{\prime}\right) d\theta^{\prime}\\ &- \left( \frac{1}{\sqrt{1-4f_{i}/\pi}} \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)\nonumber. \end{align} If we compare equations (\ref{boltzmann}) and (\ref{M_Le_boltzmann2}) we see that they are identical except for the factor $1 / \sqrt{1-4f_{i}/\pi}$ in the two components resulting from the scattering. This difference comes from the fact that, in M\&Le, multiple scattering is neglected by using an effective density, $\rho_{e}$, in lieu of the number density $\rho_{o}$. As shown in equation (\ref{rho}),

the effective density


is related to the number density as $\rho_{e}(0) = \rho_{o}/ \sqrt{1-4f_{i}/\pi}$. In summary, we have shown that, by taking the limit as the number of angles tend to infinity and as the time step $\Delta t$ tends to zero in the scattering equation of M\&Le, we obtain a linear Boltzmann equation equivalent to the equation given in \cite{jgrrealism} (once the error in this earlier work has been corrected).

\section{Determining the scattering amplitude}

The central difficulty in applying equations (\ref{boltzmann}) and (\ref{M_Le_boltzmann2}) is the determination of the scattering amplitude $D(\theta-\theta^{\prime})$. 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 \cite{jgrrealism} and M\&LE is the following. \cite{jgrrealism} assumed that the ice floes had negligible submergence but could flex, while M\&Le 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 M\&Le and \cite{jgrrealism}. Here we simply present the equation for $D(\theta)$ independent of the equation used to model the ice floe.

The water is assumed irrotational and inviscid and the wave amplitude is assumed sufficiently small that we can linearise all the equations. The water motion is represented by a velocity potential which is denoted by $\phi$. The coordinate system is the standard Cartesian coordinate system with the $z$ axis pointing vertically up. The water occupies the region $-\infty<z<0.$ We denote the free surface by $\Gamma_s$ (located at $z=0$) and the wetted surface of the ice floe by $\Gamma_w$.

The linearised boundary value problem for the fluid velocity potential $\phi({\bf r},z)$ subject to an incoming wave of frequency $\omega$ is \label{bvp} \left. \begin{array} [c]{rr}% \nabla^{2}\phi=0, & -\infty<z<0,\\ {\dfrac{\partial\phi}{\partial z}=0}, & z\rightarrow-\infty,\\

\dfrac{\partial\phi}{\partial z} = k\phi & z\in\Gamma_s \\
\dfrac{\partial\phi}{\partial z} = L\phi & z\in\Gamma_w


\end{array} \right\} % (e.g. \cite{jgrfloecirc,IJOPE04} or M\&Le). The Laplace's equation comes from the fact that the water is irrotational and inviscid. The vanishing of the normal derivative at $z=-\infty$ is the no-flow through the boundary

condition at the bottom of the infinitely deep ocean.
The condition at the free surface is the standard linear free surface


condition. 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 $L$. To actually solve equation~(\ref{bvp}) requires us to choose a specific model for the ice floe and hence to determine $L$. \cite{jgrrealism} assumed that the ice floes had negligible submergence but could flex. The solution to equation~(\ref{bvp}) for this case is described in \cite{jgrfloecirc,JGR02,IJOPE04}. M\&Le assumed the floes were rigid but allowed for submergence and the solution to equation~(\ref{bvp}) in this case is described in \cite{Masson_Le,Sarp_Isa}.

Equation (\ref{bvp}) requires boundary conditions as $x$ or $y$ tend to infinity which are found from the incident or driving wave, denoted $\phi^{\mathrmTemplate:In}$. We assume that $\phi^{\mathrmTemplate:In}$ is a plane wave travelling in the $x$ direction,

\phi^{\mathrmTemplate:In}({\bf r},z)=\frac{\omega H}{2k}e^{\rm{i}kx}e^{kz}.

The condition as $\left|\mathbf{r}\right|\rightarrow \infty$

is the standard Sommerfeld radiation condition (e.g. \cite{Weh_Lait})


\sqrt{|\mathbf{r}|}\left( \frac{\partial}{\partial|\mathbf{r}|}-\rm{i}k\right) (\phi-\phi^{\mathrmTemplate:In})=0,\;\mathrmTemplate:As\;|\mathbf{r}|\rightarrow\infty\mathrm{.} \label{sommerfield}%

Once we have found the solution to equation~(\ref{bvp}), we obtain the absolute value of the scattering amplitude $D$ as $\left\vert D\left( \theta\right) \right\vert =\frac{1}{H/2}\left( \frac {k}{2\pi}\right) ^{1/2}\left( \frac{\omega}{g}\right) \left\vert \mathbf{H}\left( \pi+\theta\right)\right\vert,$ where the Kochin function $\mathbf{H}(\tau)$ is $$\mathbf{H}(\tau)=\iint_{\Gamma_s}\left( -\frac{\delta\phi}{\delta n} + \phi\frac{\delta}{\delta n}\right) e^{kz}e^{ik(x\cos\tau +y\sin\tau)}dS,$$ where $\delta/\delta n$ is the inward normal derivative.

\section{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 $x$ spatial co-ordinate and time, i.e. there is no $y$ dependence of the solution. We also consider a uniform MIZ so that the scattering function, $S$, is a function only of $\theta$ and $\theta^{\prime}$ and $\beta$ is a constant. The only variation we allow spatially is that the MIZ occupies the region $x>b$, i.e. the ice edge is at $x=b.$ This will allow us to consider a wave spectrum which enters the MIZ from the open ocean. Under these assumptions equations (\ref{boltzmann}) and (\ref{M_Le_boltzmann2}) become, $$\frac{1}{c_{g}}\frac{\partial I}{\partial t}+\cos\theta\frac{\partial I}{\partial x}=\left\{ \begin{array} [c]{c}% \displaystyle -\beta I+\int_{0}^{2\pi}S(\theta-\theta^{\prime})I(\theta^{\prime}% )d\theta^{\prime},\;\;x>b,\\ 0,\;\;x<b. \end{array} \right. \label{almostsolvable}%$$

To solve equation (\ref{almostsolvable}) 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 $n$ angles evenly spaced between $0$ and $2\pi$ ($\theta_{j}=\frac{2\pi j}{n},\;0\leq j\leq n-1,$). This approximation converts equation (\ref{almostsolvable}) to the following equation, \frac{1}{c_{g}}\frac{\partial\vec{I}}{\partial t}-\frac{\partial}{\partial x}\mathbfTemplate:D\vec{I}=\mathbf{\left\{ \begin{array} [c]{c}% -\beta \vec{I}+\mathbf{S}\vec{I},\;\;x>b,\\ 0,\;\;x<b. \end{array} \right. } \label{matrix}% In equation (\ref{matrix}) the intensity $\vec{I}$ is now a vector of functions of $x$ and $t$ for each angle $\theta_{j}$ and the elements of the matrices $\mathbfTemplate:D$ and $\mathbfTemplate:S$ are given by, $$d_{ij}=\left\{ \begin{array} [c]{rr}% -\cos(\theta_{i}), & i=j,\\ {0,} & i\neq j, \end{array} \right.$$ and $$s_{ij}=\left\{ \begin{array} [c]{rr}% {-}\beta{+}S(\theta_{i}-\theta_{i})\frac{2\pi}{n}{,} & i=j,\\ S(\theta_{i}-\theta_{j})\frac{2\pi}{n}{,} & i\neq j, \end{array} \right.$$ respectively. Equation (\ref{matrix}) can be easily solved in the stationary (no time dependence), or isotropic (no spatial dependence) case. \cite{jgrrealism} solved the stationary problem and M\&Le solved the isotopic problem (with wind forcing etc.). In the stationary case equation (\ref{matrix}) reduces to, setting the ice edge to $b=0,$ $$-\frac{\partial}{\partial x}\mathbf{D}\vec{I}=-\beta\vec{I}+\mathbf{S}\vec{I}, \;\;x>0. \label{spaceonly}%$$ For the isotropic case, equation (\ref{matrix}) reduces to, setting the ice edge to $b=-\infty$, $$\frac{1}{c_{g}}\frac{\partial}{\partial t}\vec{I}=-\beta\vec{I}+\mathbf{S} \vec{I},\;\;t>0. \label{timeonly}%$$ Equations (\ref{spaceonly}) and (\ref{timeonly}) can be solved by straightforward matrix methods (e.g. \cite{ishimaru}). Equation (\ref{spaceonly}) requires boundary conditions (the wave spectrum at the ice edge $x=0$ and a condition as $x\to\infty$) and equation (\ref{timeonly}) requires an initial condition (the wave spectrum at $t=0$).

\section{Summary}

We have shown that the scattering theory of M\&Le can be reduced to the linear Boltzmann equation if the discrete equation is converted to a differential equation by taking the appropriate limits. We also showed that this linear Boltzmann equation is equivalent to the linear Boltzmann equation presented in \cite{jgrrealism} with an error corrected. The difference between the two theories is a term which comes from the fact that M\&Le explicitly neglected multiple scattering.

Finally, we have shown how the scattering


term is calculated from the equation of motion for an individual ice floe and how the linear Boltzmann equation can be solved in certain situations.

%\begin{acknowledgments} %This reseach was supported by the Marsden Grant UOO004. %\end{acknowledgments}