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Integrating GPS and InSAR to Measure Strain Rates along San Andreas Fault
- 1. Integrating GPS and InSAR to Measure Moment Rates along the San Andreas Fault System David T. Sandwell, Meng Wei, Xiaopeng Tong, Bridget Smith-Konter IGARSS, July 28, 2011
- 4. strain rate moment rate
- 6. strain rates from 16 groups
- 7. InSAR can resolve near-fault velocity need ~2 mm/yr precision
- 9. interseismic vector velocity model east north up [Smith-Konter and Sandwell, 2009]
- 10. locked zone Interseismic LOS Velocity high-pass filtered < 40 km ALOS has the best sensitivity to interseismic motion. ERS ascending ERS descending ALOS ascending ALOS descending [Wei et al., 2010]
- 11. locked zone Interseismic LOS Velocity high-pass filtered < 40 km Ascending ALOS has 8-20 repeats ERS/Envisat ascending ERS/Envisat descending ALOS ascending ALOS descending poor correlation poor correlation too few repeats [Wei et al., 2010]
- 12. remove/restore this LOS model
- 13. align and stack with GMTSAR unwrap phase with snaphu [Chen and Zebker, 2002]
- 15. mean LOS red 10 mm/yr blue -10mm/yr std edit > 6 mm/yr
- 16. southern SAF red 10 mm/yr blue -10mm/yr
- 17. southern SAF red 10 mm/yr blue -10mm/yr
- 18. San Jacinto stepover red 10 mm/yr blue -10mm/yr
- 19. San Jacinto stepover red 10 mm/yr blue -10mm/yr
- 20. LA Basin red 10 mm/yr blue -10mm/yr
- 21. LA Basin red 10 mm/yr blue -10mm/yr
- 22. Parkfield SAF red 10 mm/yr blue -10mm/yr
- 23. Parkfield SAF red 10 mm/yr blue -10mm/yr
- 24. Creeping SAF red 10 mm/yr blue -10mm/yr
- 25. Creeping SAF red 10 mm/yr blue -10mm/yr
- 26. Creeping SAF LOS error ~4 mm/yr
- 27. frame processing
- 28. frame processing
- 29. frame processing
- 30. frame processing
- 31. frame processing
- 32. frame processing
- 33. frame processing
- 34. frame processing
- 35. frame processing
- 36. frame processing
- 37. frame processing
- 39. interseismic model velocity strain rate moment rate = velocity depth = velocity X depth
Notas del editor
- A more accurate indication of stress loading the earthquake cycle can be given by the coulomb stress rate Explore stress accumulation due to steady slip on downward extension of variably locked faults Fault orientation varies on a segment-by-segment basis, evaluated at 1/2 local locking depth. RL shear stress, extension +, uf is effective coef. Coulomb Stress accumulation rate, which is an indication of failure conditions due to the shear traction action on a plane and the plane’s resistance to failure Rates of interseismic stress range from 0.5 - 9 MPa/100yrs and are compatible to stress rates obtained through other methodologies [Harris and Simpson, 1998]. Coulomb stress accumulates fastest in regions of shallow locking depth and high slip rate, also true of strain rate studies [Wdowinski et al., 2001] Imperial, Brawley, Parkfield, and S. Calaveras all have shallow locking depths and are optimally orientated for high stress rate (4-9 MPa/100yrs). Rates also enhanced or reduced if the fault orientation is releasing or restraining. Lower accumulation rates occur along sections where slip is partitioned on multiple strands and where locking depth is considerably deeper. (~ 15+ km) Using rec. intervals compiled by paleo-group High rates also correlate with lower recurrence interval estimates. Calculate stress drop consistent with recurrence time x coulomb stress rate, plot for 1, 5, and 10 MPa Data lay primarily with the margins of 1-7 MPa stress drop Correlation is interesting, implying that over a characteristic time period, regions accumulate sufficient amounts of tectonic stress that result in large semi-periodic earthquakes with 1-7 MPa stress drops Results are largely independent of elastic layer or viscosity of substrate - very similar results to elastic half-space model Locking depth correlation -- suggests that the tectonically induced normal stress has an important influence on depth-averaged fault strength. , accounting for the interplay of shear and normal forces acting on a fault plane, the effects of friction, fault orientation and slip direction wrt overall plate motion vector. Not absolute stress -- need in situ measurements -- stress change due to coseismic slip or interseismic strain accumulation Shear and normal stress components are resolved on a fault plane of orientation
- Fault segments vary in the depth to which they are locked throughout the interseismic period of the earthquake cycle. Apparent locking depths on each segment are adjusted to match present-day GPS measurements The nearly 1000 estimates of horizontal velocity (SCEC GPS velocity model) + SOPAC provide relatively tight constraints on locking depths: 0-26 km. RMS deviation btwn model & GPS velocity is 2.9 mm/yr (along-strike) and 1.8 mm/yr (across-strike) Large locking depths result in a broad interseismic deformation pattern, small locking depths result in a narrow pattern. While earthquake cycle effects are known to complicate estimates of true locking depth [Meade and Hager], apparent locking depth estimates, confirmed by seismicity depths, are well constrained by current GPS array