geodetic imaging of earthquake cycle processes
For the past few decades, the standard method has been Probabilistic Seismic Hazard Assessment (PSHA; The hazard models produced by PSHA are, however, only as good as the input data.
We know that frictional afterslip occurs on the shallow portions of some faults (e.g.
Over the next decade, we will see further improvement in our ability to measure tectonic deformation using satellite geodetic techniques, particularly from the combination of InSAR and GPS ( This review summarizes work conducted collaboratively with colleagues in the UK NERC's Centre for the Observation and Modelling of Earthquakes, Volcanoes and Tectonics (COMET). Firstly, plate boundary deformation zones in the continents are wide, thousands of kilometres across ( Distribution of earthquakes and GNSS velocities in the continents.
Information from three satellites gives the 3D position; data from the fourth is required because receivers on the ground don't use atomic clocks and we need to solve for the timing error.
The seismic "cycle" refers to the observation that earthquakes repeatedly rupture a given part of a fault. I will do the same, while recognizing that interseismic and postseismic deformation may be difficult to separate. All are continental strike-slip faults and all showed focused interseismic strain preceding a major earthquake and a period of rapid postseismic deformation.
The ADS is operated by the Smithsonian Astrophysical Observatory under NASA Cooperative
Firstly, they provide very accurate location information, particularly if the earthquake is shallow; there are now several examples where InSAR results have led investigators in the field to an earthquake's surface rupture.
Red colours are motion towards the satellite, whose viewing geometry is shown by the black arrow; blue colours show motion away from the satellite.
One way of addressing this question is to compare the fault slip rates derived from these simple geodetic models with those derived from geological measurements in which the fault slip rates are determined by dating surface features that have been offset by movement on the fault. This approach is challenging because the knowledge needed to make such a prediction is imperfect, and the resulting models are complex.
Geodetic observations provide kinematic constraints on the behavior of tectonically active fault systems. Those italicized occurred in the continents.
All available GNSS data have recently been compiled and analysed by Corné Kreemer and colleagues at the University of Nevada, Reno, who produced a global map of tectonic strain ( A second satellite technology, interferometric synthetic aperture radar (InSAR), can make observations of surface motions with millimetric precision, a spatial resolution of a few tens of metres, and without instruments on the ground.
The shape of that deformation indicates which parts of the upper crust are moving and at what rate. The elastic Earth acts as a natural filter, smoothing out any deformation at depth and limiting our ability to distinguish distributed shear in the lower crust and upper mantle from motion on a narrow fault plane. Maximum velocities observed are shown at the time of observation.
Earthquake cycle deformation requires a relatively strong lower crust, except near major faults – I have shown that geodetic data provide a useful complementary approach for understanding seismic hazard.
Active faults (black lines), seismicity (black/grey focal spheres) and GPS velocities (black arrows) are from Active faulting, seismicity and seismic hazard in Mongolia. One of the most significant findings from satellite geodetic measurements of fault zones is that almost all major strike-slip fault zones show focused strain around them during the interseismic period ( However, a model that fits the data is not necessarily correct.
Where points are linked, these are for the same site at the same earthquake. Each circle is an earthquake with M ≥ 6; colour denotes time of occurrence and source catalogue.
After minor corrections for any changes in the satellite's position, and provided the ground surface hasn't changed significantly in the time between the two image acquisitions, the precise topography and the changes in phase that occur when the waves interact with the ground are nearly identical in the two images.
The recovered fine-scale surface deformation leads us to better understand the underlying earthquake cycle processes.
Journal of Geophysical Research 115(B02410).
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