# Difference between revisions of "Blatter-Pattyn Boundary Conditions"

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& \hat{x}:\quad 2\eta \frac{\partial u}{\partial x}\frac{\partial s}{\partial x}+\eta \left( \frac{\partial u}{\partial y}+\frac{\partial v}{\partial x} \right)\frac{\partial s}{\partial y}-\eta \frac{\partial u}{\partial z}=-2\eta \left( \frac{\partial u}{\partial x}\frac{\partial s}{\partial x}+\frac{\partial v}{\partial y}\frac{\partial s}{\partial x} \right), \\ | & \hat{x}:\quad 2\eta \frac{\partial u}{\partial x}\frac{\partial s}{\partial x}+\eta \left( \frac{\partial u}{\partial y}+\frac{\partial v}{\partial x} \right)\frac{\partial s}{\partial y}-\eta \frac{\partial u}{\partial z}=-2\eta \left( \frac{\partial u}{\partial x}\frac{\partial s}{\partial x}+\frac{\partial v}{\partial y}\frac{\partial s}{\partial x} \right), \\ | ||

& \hat{y}:\quad 2\eta \frac{\partial v}{\partial y}\frac{\partial s}{\partial y}+\eta \left( \frac{\partial u}{\partial y}+\frac{\partial v}{\partial x} \right)\frac{\partial s}{\partial x}-\eta \frac{\partial v}{\partial z}=-2\eta \left( \frac{\partial u}{\partial x}\frac{\partial s}{\partial y}+\frac{\partial v}{\partial y}\frac{\partial s}{\partial y} \right). \\ | & \hat{y}:\quad 2\eta \frac{\partial v}{\partial y}\frac{\partial s}{\partial y}+\eta \left( \frac{\partial u}{\partial y}+\frac{\partial v}{\partial x} \right)\frac{\partial s}{\partial x}-\eta \frac{\partial v}{\partial z}=-2\eta \left( \frac{\partial u}{\partial x}\frac{\partial s}{\partial y}+\frac{\partial v}{\partial y}\frac{\partial s}{\partial y} \right). \\ | ||

+ | \end{align}</math> | ||

+ | |||

+ | |||

+ | As in the derivation of the [[1st-order stress balance equations|Blatter-Pattyn model]], collect terms of a particular velocity gradient (that is, ''u'' or ''v'') and move them to one side of the equation and, lastly, divide through by the effective viscosity ''η'' to get the final form of the 1st-order free surface boundary conditions | ||

+ | |||

+ | |||

+ | <math>\begin{align} | ||

+ | & \hat{x}:\quad 4\eta \frac{\partial u}{\partial x}\frac{\partial s}{\partial x}+\eta \frac{\partial u}{\partial y}\frac{\partial s}{\partial y}-\eta \frac{\partial u}{\partial z}=-2\eta \frac{\partial v}{\partial y}\frac{\partial s}{\partial x}-\eta \frac{\partial v}{\partial x}\frac{\partial s}{\partial y}, \\ | ||

+ | & \hat{y}:\quad 4\eta \frac{\partial v}{\partial y}\frac{\partial s}{\partial y}+\eta \frac{\partial v}{\partial x}\frac{\partial s}{\partial x}-\eta \frac{\partial v}{\partial z}=-2\eta \frac{\partial u}{\partial x}\frac{\partial s}{\partial y}-\eta \frac{\partial u}{\partial y}\frac{\partial s}{\partial x}. \\ | ||

\end{align}</math> | \end{align}</math> |

## Revision as of 21:31, 3 August 2009

We will go through an approximate derivation of the boundary conditions that are implemented with Glimmer/CISM's higher-order scheme. By "approximate" we mean that some of the derivation is guided by physical intuition and what appear to be "reasonable" arguments, rather than through the application of rigorous mathematics. We take comfort in the fact that, in the end, we wind up with the same sets of equations that one ends up with from the more rigorous approach. We will look at the derivation in three parts, (1) the free surface boundary condition, (2) the specified basal traction boundary condition, and (3) lateral boundary conditions.

## Stress Free Surface

At the ice surface, a stress-free boundary condition is applied. The traction vector, *T*, must be continuous at the ice sheet surface and, assuming that atmospheric pressure and surface tension are small, we have

where the *n _{i}* are the components of the outward facing, unit normal vector in Cartesisan coordinates.

For a function *F(x,y,z) = f(x,y) - z = 0*, where *z = f(x,y)* defines the surface, the gradient of *F(x,y,z)* gives the components of the surface normal vector:

For the case of the ice sheet surface, *s = f(x,y)* and the surface normal is given by

and

This simplification comes about because, in general, the slopes on glaciers and ice sheets are small, in which case the slope squared is very small. Thus, to first order, the surface normal vector components are simply given by

The expression above for *T _{i}=0* gives three equations that must be satisfied for a free surface boundary condition:

Expanding the last one and expressing stresses in terms of strain rates and pressures, where *η* is the effective viscosity, gives

,

which, when solved for the pressure gives

.

Expanding the above expression in terms of velocity gradients and normal vector components we have

where we have made the usual 1st-order approximation

.

Now we use this expression for the pressure and expand the two horizontal boundary condition expressions

in terms of velocity gradients and the effective viscosity to obtain

In both of these expression, the terms in square brackets are *~0* because, as noted above slopes on ice sheets are small (and the slope squared is exceedingly small). From continuity, we also have

.

Using this expression for the normal vertical velocity gradient and removing the terms in square brackets our two horizontal boundary condition expressions become

As in the derivation of the Blatter-Pattyn model, collect terms of a particular velocity gradient (that is, *u* or *v*) and move them to one side of the equation and, lastly, divide through by the effective viscosity *η* to get the final form of the 1st-order free surface boundary conditions