using gps and insar to study tectonics, deformation, and earthquakes gps displacements, velocities...
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Using GPS and InSAR to study tectonics, deformation, and
earthquakes• GPS displacements, velocities (and transients)
• InSAR displacements
Position to within about 1 cmGreat spatial coverageSensitive to vertical motionBad for high slopes or treed regionsSatellite not always looking at what you want when you wantNot so good for very large earthquakes
InSAR Displacements
McCaffrey et al., 2004http://ees2.geo.rpi.edu/rob/www/gps/gps2004.htm
GPS displacements and velocities
CGPS has sub-mm precisionCan detect rate and direction changesGood for rates and transientsNot so precise at polesVertical less precise than horizontalOnly point measurements
My research: Use GPS displacements, velocities, and transients to figure out how fault zones work at depth.
Information from seismology, geology, geochemistry and lab experiments is
also needed to build and verify models.
Method: numerical modeling.
GPS velocities in the eastern Mediterranean region
Fitting the GPS velocities with moving, rigid blocks
which ones are missing?
It’s not as simple as a bunch of rigid blocks...
D
D’
D D’
North Anatolian Fault Zone (NAFZ) has M ~7.5
earthquakes about every 300 years
fault slip!0 to 20 km depth
Non-seismic creep: 20 km depth to asthenosphere
This allows rigid translationof one plate past the other
coseismiccoseismic////postseismicpostseismic “interseismic”“interseismic”
dates and earthquake size from paleoseismology:
recent geological slip rates
dates and earthquake size from paleoseismology:
recent geological slip rates
Snapshots: GPS slip rates
Snapshots: GPS slip rates
Within an individual earthquake cycle
Within an individual earthquake cycle
Over many earthquake cycles
Over many earthquake cycles
Deformation around a plate boundary fault at different time scales
Deformation around a plate boundary fault at different time scales
Here is how interseismic deformation around a fault looks with InSAR
from Yuri Fialko’s Science paper of last summer
Colors scale with surface velocity
High strain rate means elastic stresses are building up fast
Next earthquake will be soon (or big)
Of course, last year’s EOSC 352 students knew this already....
Shear strain rate and strain rate axis orientations
From EOSC 352 Homework #5
SCEC GPS velocity field version 3
Lots can be learned from modeling interseismic deformation(beyond today’s scope)
The 1999 Izmit, Turkey earthquake:InSAR and GPS displacements
wrapped (arghh) interferogram
InSAR: like having thousands of not-too-
precise GPS sites, measuring just one
direction
Green’s function for surface displacements due to slip on a
subsurface dislocation
0 km
32 km
Slip (meters)
Slip along the NAFZ in the M = 7.5Izmit, Turkey earthquake
When the Izmit earthquake happened it
built up stresses in some areas
We can actually calculate this stress change and • model the Earth’s response to it• calculate changes in earthquake probability
on local faults
Earth models must connect episodic earthquakes with steady relative plate
motion
‘rigid’ down to asthenosphere with
localized shear zones?
creeping below mid-crust?
• This is done with creeping goo• Distribution and properties of this goo control the Earth’s response (i.e., surface motions, stress evolution)
Test the hypotheses using finite-element models
Models must reproduce the pattern and decay of
“postseismic” deformation
postseismic velocities one year after the Izmit earthquake
Model misfit to data after one year
Three years after the 1999 earthquake
Earth is still responding to the earthquake stress perturbation
Model performance: decay of postseismic velocitieslinear viscoelastic lower crust
linearly viscous shear zonevelocity-strengthening shear zone
Total modeled afterslip after a yearTotal modeled afterslip after a year
Distance along fault (km)Distance along fault (km)
Dep
th
(km
)D
ep
th
(km
)
About twice this slip would be required to fit the postseismic GPS displacements after 1 year.
About twice this slip would be required to fit the postseismic GPS displacements after 1 year.
Anatolia-Eurasia plate boundary (central NAFZ)
Eurasia
Anatolia
Moho
?
tricky rheology required?
Postseismic strain (and stressing) rates in the Marmara Sea
Postseismic strain (and stressing) rates in the Marmara Sea
coseismiccoseismic
900 days900 days
Southwest BC: Our local active faultsQueen Charlotte Fault M 8
Cascadia Subduction Zone Fault M 9.?
Faults in the subducting slab M < 7?
Shallow crustal faults M < 8
Henton et al., 2001
GPS velocity field: Vancouver Island
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