I. Introduction II. Methods in Morphotectonics III. Methods in Geodesy an Remote sensing

1. I. Introduction • II. Methods in Morphotectonics • III. Methods in Geodesy an Remote sensing • IV. Relating strain, surface displacement and stress, based on elasticity • V. Fault slip vs time • VI. Learnings from Rock Mechanics • VII. Case studies

2. IV. Relating strain, surface displacement and stress • Some elastostaticsolutions (for elastodynamic solutions see a Seismology textbook, Aki& Richard for example) • Inversion techniques • The circular crack model

3. Some classical elasticity solutions of use in tectonics • Elastic dislocations in an elastic half-space (Steketee, 1958, Cohen, Advances of geophysics, 1999; Segall) • Surface displacements due to a rectangular dislocation: Okada, 1985: • Displacements at depth due to a rectangular dislocation: Okada,1992: • The infinitely long Strike-slip fault (Segall, 2009) • 2-D model for a dip-slip fault: Manshina and Smylie, 1971, Rani and Singh, 1992; Singh and Rani, 1993, Cohen, 1996. • The Boussinesq pb (normal point load at the surface of an elastic half-space); (Jaeger, Rock mechanics and Engineering) • The Cerruti pb (shear point load at the surface of an elastic half-space); (Jaeger, Rock mechanics and Engineering) • Point source of pressure: the ‘Mogi source’(Segall, 2010) • The circular crack model (Scholz, 2002)

4. References Segall, P, Earthquake and Volcano Deformation, Princeton University Press, 2010. Scholz, C. (1990), The Mechanics of Earthquakes and Faulting, 439 pp., Cambridge University Press, New York. Cohen, S. C., Convenient formulas for determining dip-slip fault parameters from geophysical observables., Bulletin of seismological society of America, 86, 1642-1644, 1996. Cohen, S. C., Numerical models of crustal deformation in seismic zones, Adv. Geophys., 41, 134-231, 1999. Okada, Y., Surface deformation to shear and tensile faults in a half space, Bull. Seism. Soc. Am., 75, 1135-1154, 1985. Okada, Y., Internal Deformation Due To Shear And Tensile Faults In A Half-Space, Bulletin Of The Seismological Society Of America, 82, 1018-1040, 1992. Kositsky, A. P., and J. P. Avouac (2010), Inverting geodetic time series with a principal component analysis-based inversion method, Journal of Geophysical Research-Solid Earth, 115. Chanard, K., J. P. Avouac, G. Ramillien, and J. Genrich (2014), Modeling deformation induced by seasonal variations of continental water in the Himalaya region: Sensitivity to Earth elastic structure, Journal of Geophysical Research-Solid Earth, 119(6), 5097-5113.

5. In crack mechanics, 3 modes are distinguished II III I Mode I= Tensile or opening mode: displacement is normal to the crack walls Mode II= Longitudinal shear mode: displacement is in the plane of the crack and normal to the crack edge (edge dislocation) Mode III= Transverse shear mode: displacement is in the plane of the crack and parallel to the crack edge (screw dislocation)

6. Infinite Strike-Slip fault Let’s consider a fault parallel to Oy, with infinite length, and surface deformation due to uniform slip, equal to Sy, extending from the surface to a depth h. (Slip vector is (0,Sy,0) // Oy) h

7. Infinite Strike-Slip fault y x Co-seismic displacement parallel to Oy Co-seismic slip ( ,for a left-lateral fault) Co-seismic strain NB: far-field displacements and strain decay with x- 1 and x-2 respectively

8. Infinite Thrust fault Surface displacements due to slip S on a fault dipping by θ where (Manshina and Smylie, 1971; Cohen, 1996)

9. Infinite Thrust fault Surface displacements Horizontal strain Displacements are proportional to fault slip (lineraity) Note that the far-field displacements and strains decay with x- 1 and x-2

10. Infinite Thrust fault (see Cohen, 1996)

11. Convention in Okada (1985, 1992) Function [ux,uy,uz] = calc_okada(U,x,y,nu,delta,d,len,W,fault_type,strike) This function computes the displacement field [ux,uy,uz] on the grid [x,y] assuming uniform slip, on a rectangular fault with U: slip on the fault nu: Poisson Coefficient delta: dip angle d: depth of bottom edge len=2L: fault length W: fault width fault_type: 1=strike,2=dip,3=tensile,4=inflation NB:C is the middle point of bottom edge

12. Surface displacements (Okada, 1985) useful for inverting geodetic data • Displacement and strain at depth (Okada, 1992) useful for Coulomb stress change (ΔCFF) calculations

13. Observed phase It is with images of ERS acquired before and after the Landers 1992 earthquake that the first interferogram of an earthquake was produced. Massonnet et al., 1993

14. after USGS Setting of the 1992 Mw 7.3 Landers and 1999 Mw 7.1 Hector Mine Earthquakes

15. Here the measured SAR interferogram is compared with a theoretical interferogram computed based on the field measurements of co-seismic slip using the elastic dislocation theory Co-seismic displacement field due to the 1992, Landers EQ This is a validation that coseismic deformation can be modelled acurately based on the elastic dislocation theory G. Peltzer (based on Massonnet et al, Nature, 1993)

16. Co-seismic deformation during the Hector Mine earthquake Line Of Sight component of displacement Grey areas are zones of low phase coherence Courtesy of G. Peltzer, UCLA

17. The crack model works approximately in this example, In general the slip distribution is more complex than perdicted from this theory either due to the combined effects of non uniform prestress, non uniform stress drop and fault geometry. • The theory of elastic dislocations can always be used to model surface deformation predicted for any slip distribution at depth,

18. IV. 2-Inverting Surface Displacement • Principle: • Source is gridded • Linear (slip, imposed geometry) vs Nonlinear inversions (slip+geometry) • Regularisation (generally inversion is ill-posed) • Inversion of times series • ENIF (Paul Segall, Jeff McGuire) • PCAIM

19. Linear inversion • Using Green functions G calculatedwith Okada solve: • where X: geodetic displacement • S: slip on the gridded source • Laplacian Regularisation: • Weighting: - data uncertainties e.g., - λ?

20. Inversion of Time series the PCAIM technique PCAIM available on-line at: http://www.tectonics.caltech.edu/resources/pcaim (Kositsky and Avouac, JGR, 2010)

21. Inversion of Time series the PCAIM technique • Divide time series as principal components ordered amount of data variance explained • PCA and Okada Formulation are linear and associative and thus you can switch their ordering Elastic Dislocation Forward Model Elastic Dislocation Forward Model

22. Principal Components • Each component has several aspects: - Mode, time variation associated with the PC (v) • Surface Displacement, left singular value associated with the PC (u) • Singular Value, a measure of the variance of the data explained by this PC (s) • Slip Distribution, a slip map associated with the PC (l)

23. Singular Value Decomposition • First component explains maximal data variance • nth component maximal given n-1th component

24. Linear Inversion • Using Green functions G calculatedwith Okada solve:

25. Slip Decomposition of X Singular Value Decomposition + Slip Decomposition Okada Formulation =

26. Long Valley Caldara 1997-1998 Inflation Episode • multiple inflation events since 1980's • ~10 cm uplift near the resurgent dome during 1997-98 episode • 8 EDM time series • 24 ERS scene and 65 interferograms

27. Original Data SBAS Time series Electronic Distance Measurements

28. Time function Spatial function PCA Decomposition

29. PCA Reconstruction InSAR SBAS Time Series

30. Electronic Distance Measurements PCA Reconstruction

31. Joint Inversion * 1st comp only

32. Summary • PCAIM allows the joined analysis of multiple datasets with very different temporal and spatial resolutions • The approach allows to filter out tropospheric effects in the InSAR data. http://www.tectonics.caltech.edu/resources/pcaim

33. A planar circular crack of radius a with uniform stress drop,Δσ, in a perfectly elastic body (Eshelbee, 1957) The Elastic crack model Slip on the crack Stress on the crack NB: This model produces infinite stress at crack tips, which is not realistic See Pollard et Segall, 1987 or Scholz, 1990 for more details

34. The Elastic crack model A planar circular crack of radius a with uniform stress drop, Δσ, in a perfectly elastic body (Eshelbee, 1957) The predicted slip distribution is elliptical Dmean and Dmax increase linearly with fault length (if stress drop is constant). Slip on the crack Stress on the crack NB: This model produces infinite stress at crack tips, which is not realistic See Pollard et Segall, 1987 or Scholz, 1990 for more details

35. The 1999, Mw 7.1Hector Mine Earthquake N-S Component Coseismic deformation due the 1999 Mw 7.1 Hector Mine earthquake measured from 10m GSD SPOT images. Measurements of NS and EW displacement fields from the correlation of SPOT panchromatic images (pixel size 10m) taken before and after the EQ. Displacements as low of 1/10th of the pixel size (1m) can be measured from this technique (Leprince et al, 2007)

37. Δσ of the order of 5 MPa

38. (Treiman et al, 2002)

39. The 1999, Mw 7.1Hector Mine Earthquake N-S Component Coseismic deformation due the 1999 Mw 7.1 Hector Mine earthquake measured from 10m GSD SPOT images. Localized and off-fault distributed anelastic deformation add to form a smooth slip distribution (Leprince et al, 2007)