*edited 22 Feb 2015: Equations $G_{xx}^B$ and $G_{yy}^B$ corrected*

## Background of the topographic stress field calculations

The weight of mountains (or other high topography) induces stresses in the earth below the topography. Unlike many other types of stress in the crust, topographic stresses are expected to have very significant spatial variation. Therefore, in regions with high topography, it is important to include topographic stresses into the overall stress budgets of the regions.

But because of this spatial variation in topographic stresses, calculating them is not as straightforward as for some other stress components (such as lithostatic stress, which is basically $\rho g z$). As explained in the introduction, we use some techniques based on treating the earth as an elastic halfspace to calculate the stresses. Elastic halfspaces do a good job of representing appropriate (time-invariant) stresses and strains in the earth due to forcing of various sorts. They also typically have simple and well-defined solutions for how the stresses and strains from simple, well-defined perturbations (i.e. other stresses and strains) propagate throughout the halfspace.

When we calculate stresses with `halfspace`

, we use a set of these solutions
relating how a point load (force) of some known magnitude on the surface of the
halfspace induces stresses throughout the halfspace. First, we approximate
topography as a regularly-spaced array of vertical point loads
(the Digital Elevation Model we prepared a couple steps back),
and use Boussinesq's solutions for the stresses in the halfspace
resulting from the vertical point loads.

### First step: Vertical topographic forces

Boussinesq's solutions are Green's functions describing how the stresses radiate throughout a halfspace from a single, vertical point load on the surface (called $F_v$, which is equal to $-\rho g z$). The equations describe separate results for each of the six components of the stress tensor at any point in the halfspace. We will call the stresses from the vertical point sources $G^B_{ij}$, where $ij$ is the stress component of interest.

$$ G_{xx}^B = \frac{ F_v }{ 2\pi } \left[ \frac{ 3x^2 z}{ r^5 } \right. + \frac{\mu (y^2 + z^2)}{(\lambda + \mu) r^3 (z + r)} - \frac{\mu z}{(\lambda + \mu) r^3} \left. - \frac{\mu x^2}{ (\lambda + \mu) r^2 (z + r)^2 }\right ] $$

$$ G_{yy}^B = \frac{F_v}{2\pi } \left [ \frac{3y^2 z}{r^5} \right. + \frac{\mu (x^{2} + z^{2})}{(\lambda + \mu) r^{3}(z + r)} - \frac{\mu z}{(\lambda + \mu) r ^{3}} \left. - \frac{\mu y^{2}}{(\lambda + \mu ) r^2 (z +r)^2} \right] $$

$$ G_{xy}^{B} = \frac{F _{v}}{2\pi} \left[ \frac{3xyz}{r^{5}} - \frac{\mu x y (z + 2r)}{(\lambda + \mu) r^{3} (z + r)^{2}} \right] $$

$$ G_{zz}^{B} = 3 F _{v} z^{3} / 2 \pi r^{5} $$

$$ G_{xz}^{B} = 3 F _{v} xz^{2} / 2 \pi r^{5} $$

$$ G_{yz}^{B} = 3 F _{v} yz^{2} / 2 \pi r^{5} $$

*Stress components produced by a single point load*

Next, we need to go from a single point load to an array of point loads. One of the nice things about small stresses and strains in elastic halfspaces is that they are addative, so the stress field from topography is basically the sum of the stresses from the individual point loads. We could go through point by point and calculate the stress field, but there is a much better way to do it. Because of the superposition principle, we can take the sort of general solution to the Boussinesq's solution above, i.e. when $F_v=1$, and convolve this with the field of vertical forces $F_v(x,y)$, which is the DEM times density $\rho$ and gravitational force $g$, yielding the stress tensor field $M^B(x,y,z)$ (M stands for Mountain):

$$ M^B(x,y,z) = G^B(x,y,z) * F_v(x,y)$$

where $*$ is the convolution operator.

*Stress componentes from an array of point loads representing topography*

This calculation can be sped up tremendously (for large arrays) because of the [convolution theorem][conv_theor] which states that in cases like this, a convolution in the space domain is equivalent to a multiplication in the time domain. This means that we can take the Fourier transforms of both the Green's functions ($G^B$) calculated over some area, and the $F_v$ array, and then multiply those and transform the product back, instead of doing a space-domain convolution. This is great because both the Fourier transforms and the multiplication are much faster operations than the space-domain convolution.

### Next step: Horizontal topographic forces

Up to this point, the methods as described have been thought up by many scientists back to at least Harold Jeffreys. However, the result isn't quite complete. Liu and Zoback (1992) took these calculations a step further and accounted for the effects of the irregular surface above (but connected to) the halfspace into account. This includes both a correction for the horizontal shear stress induced by the effects of slope on the halfspace, and for how the irregular surface affects the propagation of stresses.

This step takes the topography and the uppermost stresses from the previous
result, and yields a field of horizontal loads $F_h(x,y)$ at the surface
of the halfspace. Then, it uses Cerruti's solutions for stresses in a halfspace
from a *horizontal* point load on the surface to propagate those stresses. The
steps are exactly the same as previously, except that the process has to be done
for horizontal loads in both the $x$ and $y$ directions. This produces a stress
field $M^C(x,y,z)$ that will be added to $M^B(x,y,z)$ to produce the final
topographic stress field $M(x,y,z)$.

The horizontal loading functions are

$$ F_{h, \, x}(x,y) = ( \rho g h(x,y) + M_{xx}^B(x,y,0) + T^0_{xx} )\, \frac{\partial h}{ \partial x} + (M_{xy}^{B}(x,y,0) + T^0_{xy}) \frac{\partial h}{ \partial y} $$

and

$$ F_{h, \, yz}(x,y) = ( \rho g h(x,y) + \sigma_{yy}^B(x,y,0) + T^0_{yy} )\, \frac{\partial h}{ \partial y} + (M_{xy}^{B}(x,y,0) + T^0_{xy}) \frac{\partial h}{ \partial x}\; . $$

Cerruti's solutions are as follows (assuming a point source loading in the $+x$ direction:

$$ G_{xx}^{C_x} = \frac{ F_{h,x} x }{2 \pi r^3} \left[ \frac{ 3x^2}{r^2} \right. - \frac{\mu}{(\lambda + \mu)(z+r)^2} \left. (r^2 - y^2 - \frac{2ry^2}{r+z}) \right] $$

$$ G_{yy}^{C_x} = \frac{ F_{h,x} x }{2 \pi r^3} \left[ \frac{ 3y^2}{r^2} \right. - \frac{\mu}{(\lambda + \mu)(z+r)^2} \left. (3r^2 - x^2 - \frac{2rx^2}{r+z}) \right] $$

$$ G_{xy}^{C_x} = \frac{ F_{h,x} x }{2 \pi r^3} \left[ \frac{ 3x^2}{r^2} \right. - \frac{\mu}{(\lambda + \mu)(z+r)^2} \left. \cdot (r^2 - x^2 - \frac{2rx^2}{r+z}) \right] $$

$$G_{zz}^{C_x} = \frac{ 3 F_{h,x} x z^2 }{2 \pi r^5}$$

$$G_{xz}^{C_x} = \frac{ 3 F_{h,x} z x^2 }{2 \pi r^5}$$

$$G_{yz}^{C_x} = \frac{ 3 F_{h,x} x y z }{2 \pi r^5}$$

These equations are then re-used, with $x$ and $y$ switched, to calculate the stresses from loads in the $y$ direction.

Here is the code to do all of this:

## Background of the topographic stress field calculations¶

The weight of mountains (or other high topography) induces stresses in the earth below the topography. Unlike many other types of stress in the crust, topographic stresses are expected to have very significant spatial variation. Therefore, in regions with high topography, it is important to include topographic stresses into the overall stress budgets of the regions.

But because of this spatial variation in topographic stresses, calculating them is not as straightforward as for some other stress components (such as lithostatic stress, which is basically $\rho g z$). As explained in the introduction, we use some techniques based on treating the earth as an elastic halfspace to calculate the stresses. Elastic halfspaces do a good job of representing appropriate (time-invariant) stresses and strains in the earth due to forcing of various sorts. They also typically have simple and well-defined solutions for how the stresses and strains from simple, well-defined perturbations (i.e. other stresses and strains) propagate throughout the halfspace.

When we calculate stresses with `halfspace`

, we use a set of these solutions
relating how a point load (force) of some known magnitude on the surface of the
halfspace induces stresses throughout the halfspace. First, we approximate
topography as a regularly-spaced array of vertical point loads
(the Digital Elevation Model we prepared a couple steps back),
and use Boussinesq's solutions for the stresses in the halfspace
resulting from the vertical point loads.

### First step: Vertical topographic forces¶

Boussinesq's solutions are Green's functions describing how the stresses radiate throughout a halfspace from a single, vertical point load on the surface (called $F_v$, which is equal to $-\rho g z$). The equations describe separate results for each of the six components of the stress tensor at any point in the halfspace. We will call the stresses from the vertical point sources $G^B_{ij}$, where $ij$ is the stress component of interest.

$$ G_{xx}^B = \frac{ F_v }{ 2\pi } \left[ \frac{ 3x^2 z }{ r^5 } \right. + \frac{\mu (y^2 + z^2)}{(\lambda + \mu) r^3 (z + r)} - \frac{\mu z}{(\lambda + \mu) r^3} \left. - \frac{\mu x^2}{ (\lambda + \mu) r^2 (z + r)^2 }\right ] $$$$ G_{yy}^B = \frac{F_v}{2\pi } \left [ \frac{3y^2 z}{r^5} \right. + \frac{\mu (x^{2} + z^{2})}{(\lambda + \mu) r^{3}(z + r)} - \frac{\mu z}{(\lambda + \mu) r ^{3}} \left. - \frac{\mu y^{2}}{(\lambda + \mu ) r^2 (z +r)^2} \right] $$$$ G_{xy}^{B} = \frac{F _{v}}{2\pi} \left[ \frac{3xyz}{r^{5}} - \frac{\mu x y (z + 2r)}{(\lambda + \mu) r^{3} (z + r)^{2}} \right] $$$$ G_{zz}^{B} = 3 F _{v} z^{3} / 2 \pi r^{5} $$$$ G_{xz}^{B} = 3 F _{v} xz^{2} / 2 \pi r^{5} $$$$ G_{yz}^{B} = 3 F _{v} yz^{2} / 2 \pi r^{5} $$
*Stress components produced by a single point load*

Next, we need to go from a single point load to an array of point loads. One of the nice things about small stresses and strains in elastic halfspaces is that they are addative, so the stress field from topography is basically the sum of the stresses from the individual point loads. We could go through point by point and calculate the stress field, but there is a much better way to do it. Because of the superposition principle, we can take the sort of general solution to the Boussinesq's solution above, i.e. when $F_v=1$, and convolve this with the field of vertical forces $F_v(x,y)$, which is the DEM times density $\rho$ and gravitational force $g$, yielding the stress tensor field $M^B(x,y,z)$ (M stands for Mountain):

$$ M^B(x,y,z) = G^B(x,y,z) * F_v(x,y)$$where $*$ is the convolution operator.

*Stress componentes from an array of point loads representing topography*

This calculation can be sped up tremendously (for large arrays) because of the [convolution theorem][conv_theor] which states that in cases like this, a convolution in the space domain is equivalent to a multiplication in the time domain. This means that we can take the Fourier transforms of both the Green's functions ($G^B$) calculated over some area, and the $F_v$ array, and then multiply those and transform the product back, instead of doing a space-domain convolution. This is great because both the Fourier transforms and the multiplication are much faster operations than the space-domain convolution.

### Next step: Horizontal topographic forces¶

Up to this point, the methods as described have been thought up by many scientists back to at least Harold Jeffreys. However, the result isn't quite complete. Liu and Zoback (1992) took these calculations a step further and accounted for the effects of the irregular surface above (but connected to) the halfspace into account. This includes both a correction for the horizontal shear stress induced by the effects of slope on the halfspace, and for how the irregular surface affects the propagation of stresses.

This step takes the topography and the uppermost stresses from the previous
result, and yields a field of horizontal loads $F_h(x,y)$ at the surface
of the halfspace. Then, it uses Cerruti's solutions for stresses in a halfspace
from a *horizontal* point load on the surface to propagate those stresses. The
steps are exactly the same as previously, except that the process has to be done
for horizontal loads in both the $x$ and $y$ directions. This produces a stress
field $M^C(x,y,z)$ that will be added to $M^B(x,y,z)$ to produce the final
topographic stress field $M(x,y,z)$.

The horizontal loading functions are

$$ F_{h, \, x}(x,y) = ( \rho g h(x,y) + M_{xx}^B(x,y,0) + T^0_{xx} )\, \frac{\partial h}{ \partial x} + (M_{xy}^{B}(x,y,0) + T^0_{xy}) \frac{\partial h}{ \partial y} $$and

$$ F_{h, \, yz}(x,y) = ( \rho g h(x,y) + \sigma_{yy}^B(x,y,0) + T^0_{yy} )\, \frac{\partial h}{ \partial y} + (M_{xy}^{B}(x,y,0) + T^0_{xy}) \frac{\partial h}{ \partial x}\; . $$Cerruti's solutions are as follows (assuming a point source loading in the $+x$ direction:

$$ G_{xx}^{C_x} = \frac{ F_{h,x} x }{2 \pi r^3} \left[ \frac{ 3x^2}{r^2} \right. - \frac{\mu}{(\lambda + \mu)(z+r)^2} \left. (r^2 - y^2 - \frac{2ry^2}{r+z}) \right] $$$$ G_{yy}^{C_x} = \frac{ F_{h,x} x }{2 \pi r^3} \left[ \frac{ 3y^2}{r^2} \right. - \frac{\mu}{(\lambda + \mu)(z+r)^2} \left. (3r^2 - x^2 - \frac{2rx^2}{r+z}) \right] $$$$ G_{xy}^{C_x} = \frac{ F_{h,x} x }{2 \pi r^3} \left[ \frac{ 3x^2}{r^2} \right. - \frac{\mu}{(\lambda + \mu)(z+r)^2} \left. \cdot (r^2 - x^2 - \frac{2rx^2}{r+z}) \right] $$$$ G^{C_x}_{zz} = \frac{ 3 F_{h,x} x z^2 }{2 \pi r^5} $$$$ G^{C_x}_{xz} = \frac{ 3 F_{h,x} z x^2 }{2 \pi r^5} $$$$ G^{C_x}_{yz} = \frac{ 3 F_{h,x} x y z }{2 \pi r^5} $$These equations are then re-used, with $x$ and $y$ switched, to calculate the stresses from loads in the $y$ direction.

## Calculating the topographic stress field¶

In this section, we calculate the 3D topographic stresses in the region below the DEM. We first calculate the vertical (Boussinesq) stresses, then the horizontal/ slope (Cerruti) correction, then add them together.

```
from __future__ import division
import numpy as np
import halfspace.load as hs
import halfspace.sandbox as hbx
import time
import h5py
import json
```

### Set some path and file names.¶

We use compressed HDF5 files for storage, using the `h5py`

library.

```
stress_dir = '../stress_arrays/'
b_stress_file = stress_dir + 'baloch_bouss_stress.h5'
c_stress_file = stress_dir + 'baloch_cerr_stress.h5'
stress_file = stress_dir + 'baloch_topo_stress.h5'
```

```
dem_file = '../test_data/dem/baloch_dem_utm41n_445m.npy'
dem_metadata_file = '../test_data/dem/baloch_dem_metadata.json'
d_meta = json.load(open(dem_metadata_file, 'r')) # DEM metadata dictionary
```

### Set up the problem¶

For the current implementation of `halfspace`

(v 0.5), topography and gravity are negative, and depth is positive. Future versions of halfspace may consider topography (above sea level) and gravity as positive; this will change the coordinate system from the current left-handed system (East, North, Down) to right-handed (East, North, Up). So check the version and release notes.

```
rho = 2700 # density in kg m^-3
g = 9.81 # gravitational force in m s^-2
Fv = - rho * g
study_res = int(d_meta['x_res_m']) # resolution for topography, filters, etc.
z_res = 1000
b_conv_mode = 'valid'
c_conv_mode = 'same'
z_min = int(d_meta['x_res_m'])
z_max = z_min + 26000
z_len = int( (z_max - z_min) / z_res + 1)
z_vec = np.linspace(z_min, z_max, num=z_len)
kernel_rad = 1.5e5
kernel_len = int( kernel_rad * 2 / study_res +1 )
kernel_shape = np.array( [kernel_len, kernel_len] )
```

#### Load topography (DEM)¶

```
print('loading')
t0 = time.time()
topo = np.load(dem_file)
topo *= -1 # new solutions use negative topo
topo_shape = topo.shape
t1 = time.time()
print('done in', t1 - t0, 's')
```

#### Optional: pad DEM for FFT convolution¶

Depending on the relative sizes of the DEM, fault, and kernel width, it may be desirable to pad the DEM prior to convolution. In our case, the fault is sufficiently far from the borders of the DEM that no padding should be necessary.

```
pad_dem = False
if pad_dem:
topo_prepad_shape = topo.shape
topo = np.pad(topo, kernel_len//2, mode='constant', constant_values=[0.])
topo_shape = topo.shape
```

## Now for the automated part.¶

All the configuration should be done above this point, and below this, the cells can simply be executed.

Therefore, when using this guide as a template to do this work for different locations, you don't need to modify anything below here.

#### Do some configuration and make empty topo stress arrays¶

```
b_out_x, b_out_y = hbx.size_output(kernel_shape, topo_shape, mode=b_conv_mode)
b_out_size = np.array( (b_out_x, b_out_y, z_len ) )
b_stress = np.empty( (b_out_size) )
b_db = h5py.File(b_stress_file)
b_dict = {}
comp_list = ['zz', 'xy', 'xz', 'yz', 'xx', 'yy']
```

### Boussinesq convolution¶

```
t2 = time.time()
for comp in comp_list:
print('working on {} stresses'.format(comp) )
b_dict[comp] = b_stress.copy()
for i, z in enumerate(z_vec):
b_dict[comp][:,:,i] = hs.do_b_convo(component=comp, z=z, Fv=Fv,
load=topo, load_mode='topo',
conv_mode=b_conv_mode,
kernel_radius=kernel_rad,
kernel_res=study_res)
b_dict[comp] *= 1e-6 # scale results to MPa
b_db.create_dataset('b_{}_MPa'.format(comp), data = b_dict[comp],
chunks = True, compression = 'gzip')
del b_dict[comp]
print('done with Boussinesq calcs in', (time.time() - t2) / 60., 'm')
```

### Cerruti convolution¶

#### Calculate horizontal loading functions¶

```
# Boussinesq stresses for xx, xy and yy are used in the loading function
b_xx_top = b_db['b_xx_MPa'][:,:,0] * 1e6
b_xy_top = b_db['b_xy_MPa'][:,:,0] * 1e6
b_yy_top = b_db['b_yy_MPa'][:,:,0] * 1e6
b_shape = b_xx_top.shape
topo = hs._centered(topo, b_shape)
topo_dy, topo_dx = np.gradient(topo, study_res)
```

```
# make horizontal loading functions
Fht_x = topo * Fv * topo_dx
Fhb_x = b_xx_top * topo_dx + b_xy_top * topo_dy
Fht_y = topo * Fv * topo_dy
Fhb_y = b_yy_top * topo_dy + b_xy_top * topo_dx
Fh_x = Fht_x + Fhb_x
Fh_y = Fht_y + Fhb_y
```

```
# make Cerruti output arrays
c_x = np.zeros([topo.shape[0], topo.shape[1], z_len])
c_y = c_x.copy()
c_db = h5py.File(c_stress_file)
t_db = h5py.File(stress_file)
del topo # save some ram
cerr_x = {}
cerr_y = {}
total_dict = {}
```

### Do Cerruti convolutions¶

```
t3 = time.time()
for comp in comp_list:
print('working on {} stresses'.format(comp))
cerr_x[comp] = c_x.copy()
cerr_y[comp] = c_y.copy()
for i, z in enumerate(z_vec):
cerr_x[comp][:,:,i] = hs.do_c_convo(component=comp, f_dir='x',z=z,
load=Fh_x, kernel_res=study_res,
kernel_radius=kernel_rad,
conv_mode=c_conv_mode) * 1e-6
cerr_y[comp][:,:,i] = hs.do_c_convo(component=comp, f_dir='y', z=z,
load=Fh_y, kernel_res=study_res,
kernel_radius=kernel_rad,
conv_mode=c_conv_mode) * 1e-6
print('saving {} data'.format(comp))
c_db.create_dataset('c_{}_x_MPa'.format(comp),
data = cerr_x[comp], chunks=True, compression = 'gzip')
c_db.create_dataset('c_{}_y_MPa'.format(comp),
data = cerr_y[comp], chunks=True, compression = 'gzip')
print('adding all results together')
total_dict[comp] = (b_db['b_{}_MPa'.format(comp)][:,:,:] + cerr_x[comp]
+ cerr_y[comp] )
t_db.create_dataset('{}_MPa'.format(comp), data=total_dict[comp],
chunks = True, compression = 'gzip')
del total_dict[comp]
del cerr_x[comp]
del cerr_y[comp]
print('done with topo corrections in', (time.time() - t3) / 60., 'm')
```

### Close HDF5 files¶

```
b_db.close()
c_db.close()
t_db.close()
```

```
print('done in', (time.time() - t0) / 60., 'm')
```

## Done!¶

The files `baloch_cerr_stress.h5`

and `baloch_bouss_stress.h5`

take up a lot of room, and may be deleted, unless inspection of them is desired (and if so, it may be simpler to just generate them again, rather than keep ~3-8 GB (depending on padding) of somewhat useless data on hand).

## Table of Contents for the `halfspace`

tutorial

- Installation and configuration
- Preparing a Digital Elevation Model file
- Preparing the coseismic slip model
- Calculating the topographic stress field
- Calculating the topographic stresses on the fault
- Bayesian inversion of tectonic stress pt. 1: Rake inversion
- Bayesian inversion of tectonic stress pt. 2: Conditions at failure