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

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& i=x:\quad T_{x}=\sigma _{xx}n_{x}+\sigma _{xy}n_{y}+\sigma _{xz}n_{z}=0, \\ | & i=x:\quad T_{x}=\sigma _{xx}n_{x}+\sigma _{xy}n_{y}+\sigma _{xz}n_{z}=0, \\ | ||

& i=y:\quad T_{y}=\sigma _{yx}n_{x}+\sigma _{yy}n_{y}+\sigma _{yz}n_{z}=0, \\\end{align}</math> | & i=y:\quad T_{y}=\sigma _{yx}n_{x}+\sigma _{yy}n_{y}+\sigma _{yz}n_{z}=0, \\\end{align}</math> | ||

+ | |||

in terms of velocity gradients and the effective viscosity to obtain | in terms of velocity gradients and the effective viscosity to obtain | ||

+ | |||

+ | |||

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

+ | {} & \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}= \\ | ||

+ | {} & \quad \quad \quad \quad \quad 2\eta \frac{\partial w}{\partial z}\frac{\partial s}{\partial x}-\eta \frac{\partial u}{\partial z}\left[ \frac{\partial s}{\partial x}\frac{\partial s}{\partial x} \right]-\eta \frac{\partial v}{\partial z}\left[ \frac{\partial s}{\partial y}\frac{\partial s}{\partial x} \right], \\ | ||

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

+ | |||

+ | |||

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

+ | {} & \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}= \\ | ||

+ | {} & \quad \quad \quad \quad \quad 2\eta \frac{\partial w}{\partial z}\frac{\partial s}{\partial y}-\eta \frac{\partial u}{\partial z}\left[ \frac{\partial s}{\partial x}\frac{\partial s}{\partial y} \right]-\eta \frac{\partial v}{\partial z}\left[ \frac{\partial s}{\partial y}\frac{\partial s}{\partial y} \right]. \\ | ||

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

+ | |||

+ | |||

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

+ | |||

+ | |||

+ | <math>\frac{\partial w}{\partial z}=-\frac{\partial u}{\partial x}-\frac{\partial v}{\partial y}</math>. | ||

+ | |||

+ | |||

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

+ | |||

+ | |||

+ | |||

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

+ | {} & \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). \\ | ||

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

==Specified Basal Traction== | ==Specified Basal Traction== |

## Revision as of 00:34, 11 March 2011

We will go through an approximate derivation of the boundary conditions that are implemented with CISM's higher-order scheme. By "approximate" we mean that some of the derivation is guided by physical intuition and reasonable arguments, rather than through the application of rigorous mathematics. In the end, we wind up with the same set of equations that one ends up with from the more rigorous approach (see, e.g. *Dukowicz et al.*,2010. 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.

## Contents |

## 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) = z - f(x,y) = 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

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 that

.

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

## Specified Basal Traction

Derivation of the basal boundary condition follows that above for the free surface except that (1) the right-hand side of the equation is not zero, rather it consists of an assumed basal traction vector with components , (2) the normal vector components now consist of horizontal gradients in the basal surface, and (3) the effective viscosity does not disappear from the equations when we divide through. Making these substitutions we obtain the 1st-order basal boundary conditions for a specified basal traction

We assume that basal traction is related to basal sliding velocity through a traction paramter, *β*, such that

.

Substituting this expression into the above gives our final horizontal boundary conditions at the ice sheet base

## Specified Basal Yield Stress

The above implementation of a specified basal traction can be altered to simulate sliding over a "plastic" bed. That is, sliding does not occur below the specified yield stress of the underlying material (e.g. a subglacial till). When the yield stress, *τ _{0}* is reached, sliding occurs at a rate that maintains that yield stress. Consider the

*x*direction boundary condition above, written out in terms of basal stress components,

In the expression above, *u* is the *x* component of velocity from the current iteration, *u _{0}* and

*v*are velocity components from the previous iteration, and

_{0}*γ*is a regularization constant (a small constant number to avoid division by zero during early iterations). Note that as the solution converges, velocities at the current and previous iteration are nearly equal, and the expression in parentheses approaches 1, in which case the basal stress and yield stress are approximately equal.

We can easily accommodate this in our earlier framework for incorporating the traction parameter *β* by treating *β* as nonlinear and dependent on the velocity,

.

Thus, we can implement plastic bed sliding behavior simply by substituting the above expression for our "nonlinear" *β* into our previous expressions for the basal boundary conditions in *x* (a similar expression applies for the *y* direction). The Figures below show some examples of this type of boundary condition for the case of an idealized ice stream.

**Figure 1:** Idealized ice stream with plastic-bed sliding. Top panel shows a schematic of an idealized ice stream, frozen at the margins and thawed within the ice stream (flow is out of the page). Bottom panel (color) shows a modeled, idealized ice stream (flow is from left to right) with a yield stress of 5 kPa within the ice stream and much larger than 5 kPa outside of it. Bottom left shows the ice stream speed and the bottom right shows the basal drag. Within the ice stream basal drag is equal to the yield stress. Outside of the ice stream, stress transfer to the lateral margins results in basal drag that is much larger than the yield stress (and much larger than the driving stress).

**Figure 2:** Across-flow profiles of velocity and basal drag from the modeled, idealized ice stream in Figure 1. In the top panel, the analytical solution from *Raymond* (2005) is also shown for comparison. In the bottom panel, stress transfer to the lateral margins is clearly seen.

## Lateral Boundary Conditions

Currently, the only lateral boundary condition implemented that is of any significance is that for floating ice; the depth-averaged stress resulting from an adjacent column of ocean water is applied at the location of an ice shelf (or ice tongue) front. The derivation follows largely along the lines above for the free surface and specified basal traction boundary conditions, except that the surface normal vectors, nx and ny, are taken as lying entirely in the x, y plane (that is, they are perpendicular to a vertical shelf front). Thus we have

where *S _{x}* and

*S*are source terms from the pressure due to ocean water (to be defined below) and comes from including the 1st order vertical stress balance

_{y}

with *ρ* being the ice density. In the last step above we have used the constitutive relation and incompressibility to expand the vertical, normal-deviatoric stress in terms of the effective viscosity and horizontal-normal strain rates. We calculate the source terms *S _{x}* and

*S*as the depth-averaged stress at the ice shelf front due to the pressure of ocean water there. This value is given by

_{y}

where *i=x,y*, *n _{i}* is the shelf-front normal vector,

*H*is the ice thickness,

*h*is the “freeboard”, or ice thickness above floatation, and

*ρ*is the density of ocean water. Because we’ve taken a depth-average for this source term, we take a depth-average of the term above, which is . Combining these two terms and inserting them in the horizontal boundary condition expressions above gives

_{w}

which can be rearranged to

For an ice shelf, the surface and basal velocities are equal, in which case the vertical velocity gradient terms are ~0, giving the final form of the boundary conditions implemented in the model,

.

## Summary

You may have noticed that the form of ALL of the boundary conditions above is very similar. In fact, all that differs among the equations for the free surface, the specified basal traction, and the lateral shelf boundary condition is (1) the definition of the normal vectors and (2) the existence and definition of a source term. Here are the *x* direction equations again for the three cases:

In the first equation (free surface), the normals are related to the ice sheet surface slope and the source term is zero (which subsequently allows us to divide through by the effective viscosity and remove it from the equations). In the second equation (specified basal traction), the normals are related to the bedrock slopes and the source term is related to the basal shear stress. In the last equation, the normals are defined by the shape of the ice-shelf front in map view and the source term is related to the pressure from the adjacent column of ocean water.

Continue with the Solution of the Blatter-Pattyn model.

Return to Blatter-Pattyn model.

Return to Higher order velocity schemes.