From Interactive System for Ice sheet Simulation


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−  The starting point for the BlatterPattyn model is the full Stokes equations
 
   
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−  <math>\begin{align}
 
−  & x:\quad \frac{\partial \tau _{xx}}{\partial x}\frac{\partial P}{\partial x}+\frac{\partial \tau _{xy}}{\partial y}+\frac{\partial \tau _{xz}}{\partial z}=0 \\
 
−  & y:\quad \frac{\partial \tau _{yy}}{\partial y}\frac{\partial P}{\partial y}+\frac{\partial \tau _{xy}}{\partial x}+\frac{\partial \tau _{yz}}{\partial z}=0 \\
 
−  & z:\quad \frac{\partial \tau _{zz}}{\partial z}\frac{\partial P}{\partial z}+\frac{\partial \tau _{zy}}{\partial y}+\frac{\partial \tau _{xz}}{\partial x}=\rho g \\
 
−  \end{align}</math>,
 
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−  where ''P'' is the pressure and <big>τ</big> is the deviatoric stress tensor. The latter is given by
 
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−  <big><math>\tau _{ij}=\sigma _{ij}+P\delta _{ij}</math></big>,
 
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−  where <big>σ</big> is the full stress tensor.
 
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−  There are a number of ways to argue that because of the "shallowness" of ice sheets  that is because the ratio of <big>''H''/''L''</big>, where ''H'' is the thickness and ''L'' is a relevant horizontal length scale, is small  the equations above can be reduced to the following "firstorder approximation"
 
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−  <math>\begin{align}
 
−  & x:\quad \frac{\partial \tau _{xx}}{\partial x}\frac{\partial P}{\partial x}+\frac{\partial \tau _{xy}}{\partial y}+\frac{\partial \tau _{xz}}{\partial z}=0 \\
 
−  & y:\quad \frac{\partial \tau _{yy}}{\partial y}\frac{\partial P}{\partial y}+\frac{\partial \tau _{xy}}{\partial x}+\frac{\partial \tau _{yz}}{\partial z}=0 \\
 
−  & z:\quad \frac{\partial \tau _{zz}}{\partial z}\frac{\partial P}{\partial z}=\rho g \\
 
−  \end{align}</math>
 
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−  Unfortunately, the arguments that support this reduction are complex and we can't go into them in detail here. Two papers given in the references below (''Schoof and Hindmarsh'' (in press) and ''Dukowicz et al.'' (submitted)) provide more details on the mathematical background that allows us to state that these equations are "first order accurate" approximations to the Stokes equations.
 
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−  We continue by noting that the 3rd (vertical) balance equation above can be integrated through the depth of the ice sheet to give an expression for the pressure, ''P'',
 
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−  <math>P=\rho g\left( sz \right)+\tau _{zz}(z)</math>
 
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−  This expression can be substituted into the horizontal pressure gradient terms above to remove pressure from the equations. For example, for the 'x' component of velocity we have
 
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−  <math>\begin{align}
 
−  & x:\quad \frac{\partial \tau _{xx}}{\partial x}+\frac{\partial \tau _{xy}}{\partial y}+\frac{\partial \tau _{xz}}{\partial z}=\frac{\partial P}{\partial x} \\
 
−  & x:\quad \frac{\partial \tau _{xx}}{\partial x}+\frac{\partial \tau _{xy}}{\partial y}+\frac{\partial \tau _{xz}}{\partial z}=\frac{\partial }{\partial x}\left[ \rho g\left( sz \right)+\tau _{zz}(z) \right] \\
 
−  & x:\quad \frac{\partial \tau _{xx}}{\partial x}\frac{\partial \tau _{zz}}{\partial x}+\frac{\partial \tau _{xy}}{\partial y}+\frac{\partial \tau _{xz}}{\partial z}=\rho g\frac{\partial s}{\partial x} \\
 
−  \end{align}</math>
 
Revision as of 16:59, 30 July 2009