[CIG-SHORT] RELAX Question

[Austin Madson]

Prof. Barbot,

Thanks for the well written explanation!

Before I move on to viscous layers, I ran a sanity check (see below) to get
the response from a 2.44m water level increase in a lake. The response was
much higher than anticipated (~19cm where it should be <2cm). Is RELAX not
set up to properly look at elastic outputs (Which is fine, because I'm
after viscoelastic outputs). But, if the initial elastic response is this
high I'm concerned the viscoelastic response will still be too great (with
a tau = ~ 10-13 years)). I'm quite certain everything is correct here. What
do you think? I have attached a PDF from the output as well.

Thanks in advance!

Also, do you know anyone using RELAX for surface loading?

Cheers,
Austin M

Lamé params in GPa, load in MPa, sampling in km.

# grid dimension (sx1,sx2,sx3)
512 512 512
# sampling (dx1,dx2,dx3), smoothing (beta, nyquist)
0.9765625 0.9765625 0.9765625 0.2 0
# origin position (x0,y0) and rotation
0 0 0
# observation depth (displacement and stress)
0 0
# output directory
$WDIR
# lambda, mu, gamma (gamma = (1 - nu) rho g / mu)
30 30 8.33e-4
# time interval, (positive time step) or (negative skip, scaling)
0 1 1
# number of observation planes
0
# number of observation points
0
# number of stress observation segments
0
# number of prestress interfaces
0
# number of linear viscous interfaces
0
# number of nonlinear viscous interfaces
0
# number of fault creep interfaces
0
# number of inter-seismic strike-slip segments
0
# number of inter-seismic tensile segments
0
# number of events
1
# number of coseismic strike-slip segments
0
# number of coseismic tensile segments
0
# number of coseismic dilatation point sources
0
# number of surface loads
#890730
2
# nb x1 x2 length(x) width(y) t3 T phi (t3 in MPa)
1 15 -15 30 30 0.023912  0 0
2 10 -35 20 20 0.023912  0 0
EOF




On Tue, Jan 26, 2016 at 3:07 PM, Sylvain Barbot <sylbar.vainbot at gmail.com>
wrote:

> Hi Austin,
>
> If your spatial sampling is in km then your Lamé parameters are in GPa,
> your load in MPa and your displacement in meters. If your spatial sampling
> was in meters, then your Lamé parameters and your load would be in GPa (or
> more precisely, the same, arbitrary, unit). The difference comes from
> stress being rigidity times strain, and strain being displacement divided
> by distance. If the distance and displacements are not in the same units,
> you bias the strain.
>
> Cheers,
> Sylvain
>
>
> On Wednesday, January 27, 2016, Austin Madson <amadson at ucla.edu> wrote:
>
>> Prof. Barbot,
>>
>> Thanks again for the response. Just to confirm, if in the below example
>> (the same as before) the Lamé params are in GPa (30 and 30) then t3 would
>> be in GPa (of the load) and the output surface displacement would still be
>> in meters?
>>
>> Thanks!!
>>
>> Cheers,
>> Austin M
>>
>>
>> # grid dimension (sx1,sx2,sx3)
>> 512 512 512
>> # sampling (dx1,dx2,dx3), smoothing (beta, nyquist)
>> 0.9765625 0.9765625 0.9765625 0.2 0
>> # origin position (x0,y0) and rotation
>> 0 0 0
>> # observation depth (displacement and stress)
>> 0 0
>> # output directory
>> $WDIR
>> # lambda, mu, gamma (gamma = (1 - nu) rho g / mu)
>> 30 30 8.33e-4
>> # time interval, (positive time step) or (negative skip, scaling)
>> 1 1 1
>> # number of observation planes
>> 0
>> # number of observation points
>> 0
>> # number of stress observation segments
>> 0
>> # number of prestress interfaces
>> 0
>> # number of linear viscous interfaces
>> 0
>> # number of nonlinear viscous interfaces
>> 0
>> # number of fault creep interfaces
>> 0
>> # number of inter-seismic strike-slip segments
>> 0
>> # number of inter-seismic tensile segments
>> 0
>> # number of events
>> 1
>> # number of coseismic strike-slip segments
>> 0
>> # number of coseismic tensile segments
>> 0
>> # number of coseismic dilatation point sources
>> 0
>> # number of surface loads
>> 1
>> # nb x1 x2 length width t3 T phi
>> 1 0 0 3.937 3.937 20 0 0
>> EOF
>>
>> On Fri, Jan 22, 2016 at 4:30 AM, Sylvain Barbot <sylbar.vainbot at gmail.com
>> > wrote:
>>
>>> Hi Austin,
>>>
>>> With your input file, you compute the displacement field at the
>>> surface with units of meters, due to a 4x4 km patch where a load of 20
>>> MPa is applied. Your spatial sampling is 4 km. The value of gamma
>>> should be 8.33e-4 in units of 1/km.
>>>
>>> Cheers,
>>> Sylvain
>>>
>>> On Fri, Jan 22, 2016 at 4:24 PM, Austin Madson <amadson at ucla.edu> wrote:
>>> > Prof. Barbot,
>>> >
>>> > Thanks again for the response - you've been  very helpful thusfar.
>>> >
>>> > Just to confirm:
>>> > Trying to get at displacement units (let's call them km). If my inputs
>>> are
>>> > the following, and I divide out the 1e3 from the displacement field -
>>> the
>>> > units are just that, km. Is that correct? Or, if I keep the Lamé
>>> parameters
>>> > (along with t3)  in GPa instead of kPa - does the Gamma value then =
>>> 8.33e2
>>> > [gamma=8.33e2 = (1-0.25)*3400*9.8/30 or gamma=8.33e4 =
>>> > (1-0.25)*3400*9.8/30000000 ],  and we still divide out the 1e3 from the
>>> > displacement to get the units in "km"?
>>> >
>>> >
>>> >
>>> > Cheers and thanks!
>>> >
>>> > Austin M
>>> >
>>> >
>>> >
>>> >
>>> > # grid dimension (sx1,sx2,sx3)
>>> > 512 512 512
>>> > # sampling (dx1,dx2,dx3), smoothing (beta, nyquist)
>>> > 0.9765625 0.9765625 0.9765625 0.2 0
>>> > # origin position (x0,y0) and rotation
>>> > 0 0 0
>>> > # observation depth (displacement and stress)
>>> > 0 0
>>> > # output directory
>>> > $WDIR
>>> > # lambda, mu, gamma (gamma = (1 - nu) rho g / mu)
>>> > 30 30 8.33e-4
>>> > # time interval, (positive time step) or (negative skip, scaling)
>>> > 1 1 1
>>> > # number of observation planes
>>> > 0
>>> > # number of observation points
>>> > 0
>>> > # number of stress observation segments
>>> > 0
>>> > # number of prestress interfaces
>>> > 0
>>> > # number of linear viscous interfaces
>>> > 0
>>> > # number of nonlinear viscous interfaces
>>> > 0
>>> > # number of fault creep interfaces
>>> > 0
>>> > # number of inter-seismic strike-slip segments
>>> > 0
>>> > # number of inter-seismic tensile segments
>>> > 0
>>> > # number of events
>>> > 1
>>> > # number of coseismic strike-slip segments
>>> > 0
>>> > # number of coseismic tensile segments
>>> > 0
>>> > # number of coseismic dilatation point sources
>>> > 0
>>> > # number of surface loads
>>> > 1
>>> > # nb x1 x2 length width t3 T phi
>>> > 1 0 0 3.937 3.937 20 0 0
>>> > EOF
>>> >
>>> >
>>> > On Tue, Jan 19, 2016 at 11:20 PM, Sylvain Barbot <
>>> sylbar.vainbot at gmail.com>
>>> > wrote:
>>> >>
>>> >> Hi Austin,
>>> >>
>>> >> I often get questions about units. There are no formal choice of units
>>> >> in Relax, except that S.I. units, or more precisely, their
>>> >> inter-relationships, is assumed. The expected input of the current
>>> >> version of Relax is
>>> >>
>>> >> n x1 x2 length width t3 T phi
>>> >>
>>> >> where n is the index, x1 and x2 and north and east, length and width
>>> >> are the dimension of the source patch, t3 is the traction (force per
>>> >> unit area), and T and phi is the period and phase assuming the
>>> >> following model
>>> >>
>>> >> p(t)=t3*sin(2*pi*t/period+phi)
>>> >>
>>> >> t3 is the load in units of stress. If you prescribed your Lamé
>>> >> parameters in units of MPa, you need to describe the load in MPa.
>>> >>
>>> >> I apologise that the examples I sent you correspond to an old version
>>> >> of Relax. The current version assumes stress units. (The previous
>>> >> version expected t3/G.) The factor of 1,000 comes in depending on your
>>> >> choice of length units. If you use km, it introduces a factor of 1,000
>>> >> in the displacement field. You can compensate this effect by dividing
>>> >> the rigidity by the same factor.
>>> >>
>>> >> Cheers,
>>> >> Sylvain
>>> >>
>>> >>
>>> >> On Wed, Jan 20, 2016 at 2:03 PM, Austin Madson <amadson at ucla.edu>
>>> wrote:
>>> >> > Prof. Barbot,
>>> >> >
>>> >> > Thanks for the response and the example data. I am working out my
>>> >> > parameters
>>> >> > (and units now). I think I have a lock on the elastic and
>>> viscoelastic
>>> >> > params. However, I am having trouble with the load parameters.
>>> >> >
>>> >> > I see that on some of your input files the surface load/traction
>>> >> > parameters
>>> >> > are;
>>> >> > nb x1 x2 length width t3 T phi
>>> >> >
>>> >> > and another has;
>>> >> > nb x1 x2 t3 length width T phi
>>> >> >
>>> >> > I assume the former is correct, yes?
>>> >> >
>>> >> > Also, I'm trying to wrap my head around the units for force(t3). In
>>> the
>>> >> > GRACE example (the _km.xyz file), the z is used in the following
>>> >> > calculation
>>> >> > ($3*9.8/3e10) in order to get force(t3). What are the initial units
>>> in
>>> >> > the
>>> >> > _km.xyz file for the third column, z? And what are the units after
>>> the
>>> >> > calculation ($3*9.8/3e10) in order to derive force(t3)?
>>> >> >
>>> >> > Also, it appears that the output vertical (z) displacement units
>>> are in
>>> >> > mm,
>>> >> > may I assume that is correct?
>>> >> >
>>> >> > Cheers and thanks A LOT for your responses!
>>> >> > Austin M
>>> >> >
>>> >> > On Tue, Jan 19, 2016 at 9:29 AM, Sylvain Barbot
>>> >> > <sylbar.vainbot at gmail.com>
>>> >> > wrote:
>>> >> >>
>>> >> >> Hi Austin,
>>> >> >>
>>> >> >> The Tibet lakes have a great loading signal. You can use Relax to
>>> >> >> simulate the deformation, but you need to be careful about how
>>> >> >> important the elastic stratification is. If your data are close to
>>> the
>>> >> >> source, you're fine. I presume you are using paleo-shoreline data.
>>> If
>>> >> >> so, use the shallow rigidity for the entire domain. If you are
>>> >> >> modeling far-field data, you should use a code that have a layered
>>> >> >> elastic structure, i.e., (Farrell, 1972).
>>> >> >>
>>> >> >> The example attached models the deformation from the Indian monsoon
>>> >> >> using Grace data. The example cycleload.sh creates a periodic
>>> surface
>>> >> >> load.
>>> >> >>
>>> >> >> Best wishes,
>>> >> >> Sylvain
>>> >> >>
>>> >> >>
>>> >> >>
>>> >> >> On Tue, Jan 19, 2016 at 10:51 AM, Austin Madson <amadson at ucla.edu>
>>> >> >> wrote:
>>> >> >> > Professor Barbot,
>>> >> >> >
>>> >> >> > Thanks for the prompt response. I looked at the documentation
>>> and the
>>> >> >> > man
>>> >> >> > page (as well as the examples on the PDF on the geodynamics
>>> website)
>>> >> >> > and
>>> >> >> > have made progress.
>>> >> >> >
>>> >> >> > As an fyi, we plan on modeling several hundred years of surface
>>> >> >> > loading
>>> >> >> > from
>>> >> >> > very large lakes (i.e. time dependent loads). Are there any RELAX
>>> >> >> > surface
>>> >> >> > load examples laying around (they can just be single/multiple
>>> point
>>> >> >> > and
>>> >> >> > even
>>> >> >> > instantaneous (no time function)? The GRACE example on the
>>> example
>>> >> >> > pdf
>>> >> >> > "hides" the data in various dat files (which makes sense if
>>> you're
>>> >> >> > using
>>> >> >> > a
>>> >> >> > lot of data, but it's hard to see their example inputs).
>>> >> >> >
>>> >> >> > I expect to see only millimeters of deformation throughout the
>>> run -
>>> >> >> > will
>>> >> >> > the outputs be precise enough if I use the correct SI units
>>> >> >> > throughout?
>>> >> >> >
>>> >> >> > Cheers,
>>> >> >> > Austin Madson
>>> >> >> >
>>> >> >> > On Sun, Jan 17, 2016 at 4:06 PM, Sylvain Barbot
>>> >> >> > <sylbar.vainbot at gmail.com>
>>> >> >> > wrote:
>>> >> >> >>
>>> >> >> >> Hi Austin,
>>> >> >> >>
>>> >> >> >> The details of the input file for surface loads are in the
>>> >> >> >> documentation
>>> >> >> >> and in the man page. There are some pdf files on the geodynamics
>>> >> >> >> website
>>> >> >> >> that show examples of surface loads for the Himalayan region if
>>> I
>>> >> >> >> recall
>>> >> >> >> well.
>>> >> >> >>
>>> >> >> >> But the input file simply expects a list of squares with their
>>> >> >> >> associated
>>> >> >> >> traction. So depending on your project, this can be a single
>>> point,
>>> >> >> >> say
>>> >> >> >> to
>>> >> >> >> represent the loading of a dam, or a complicated function of
>>> space
>>> >> >> >> and
>>> >> >> >> time.
>>> >> >> >> If your change of load is instantaneous, you need only one
>>> event. Of
>>> >> >> >> your
>>> >> >> >> load is time dependent, you need as many events as you have time
>>> >> >> >> steps.
>>> >> >> >> I
>>> >> >> >> can be more specific, but I need more information about your
>>> >> >> >> practical
>>> >> >> >> goals.
>>> >> >> >>
>>> >> >> >> Cheers,
>>> >> >> >> Sylvain
>>> >> >> >>
>>> >> >> >>
>>> >> >> >> On Monday, January 18, 2016, Austin Madson <amadson at ucla.edu>
>>> wrote:
>>> >> >> >>>
>>> >> >> >>> Professor Barbot,
>>> >> >> >>>
>>> >> >> >>> I have a quick question re: RELAX - Is there any more
>>> information
>>> >> >> >>> out
>>> >> >> >>> there with respect to utilizing RELAX for deformation
>>> responses to
>>> >> >> >>> surface
>>> >> >> >>> loading? I have looked through all of the examples as well as
>>> the
>>> >> >> >>> slides/tutorials on the geodynamics.org website.
>>> >> >> >>>
>>> >> >> >>> Can you provide any further information? Or can you point me
>>> in a
>>> >> >> >>> better
>>> >> >> >>> direction?
>>> >> >> >>>
>>> >> >> >>> Cheers,
>>> >> >> >>> Austin Madson
>>> >> >> >
>>> >> >> >
>>> >> >
>>> >> >
>>> >
>>> >
>>>
>>
>>
-------------- next part --------------
An HTML attachment was scrubbed...
URL: <http://lists.geodynamics.org/pipermail/cig-short/attachments/20160127/53edb9a5/attachment-0001.html>
-------------- next part --------------
A non-text attachment was scrubbed...
Name: 000-up.grd-plot.pdf
Type: application/pdf
Size: 25244 bytes
Desc: not available
URL: <http://lists.geodynamics.org/pipermail/cig-short/attachments/20160127/53edb9a5/attachment-0001.pdf>