IV. The seismic cycle

1. IV. The seismic cycle IV. 1 Conceptual and kinematic models IV.2 Comparison with observations IV.3 Interseismic strain IV.4 Postseismic deformation IV.5 Dynamic models

2. Source Model of Nias Earthquake Source duration: 100s, Rupture velocity: 2-2.5 km/s; Rise time: 15 sec (Konca et al, 2007)

3. Postseismic deformationover 11 months

4. Time evolution of postseismic slip • The spatial distribution of afterslip is approximately stationary. • Slip increases in proportion to the logarithm of time (Hsu et al, 2006) ~

5. Alaska: ~ 40 years after a great earthquake M = 9.2, 1964 Freymueller et al. (2008) The plate interface has partially or completely relocked in the rupture area. Some stations on land still move seaward!

6. M = 9.5, 1960 Chile: ~ 40 years after a great earthquake GPS data: Green: Klotz et al. (2001) Red: Wang et al. (2007) (From Kelin Wang, SEIZE meeting, 2008; Wang, 2007)

7. Wells and Simpson (2001) Cascadia: ~ 300 years after a great earthquake (From Kelin Wang, SEIZE meeting, 2008; Wang, 2007)

8. Afterslip Stress relaxation Stress relaxation Locking Rupture Afterslip and transient slow slip: short-lived, fault friction Stress relaxation: long-lived, mantle rheology (From Kelin Wang, SEIZE meeting, 2008; Wang, 2007)

9. References Hsu, Y. J., M. Simons, J. P. Avouac, J. Galetzka, K. Sieh, M. Chlieh, D. Natawidjaja, L. Prawirodirdjo, and Y. Bock (2006), Frictional afterslip following the 2005 Nias-Simeulue earthquake, Sumatra, Science, 312(5782), 1921-1926. Wang, K, Elastic and Viscoelastic Models of Crustal Deformation in Subduction Earthquake Cycles, In The Seismogenic Zone of Subduction Thrust Faults, edited by T. Dixon and J. C. Moore, Columbia University Press, 2007 .

10. IV. The seismic cycle IV. 1 Conceptual and kinematic models IV.2 Comparison with EQ observations IV.3 Learning from interseismic strain IV.4 Dynamic models

11. Kinematic model : the model is parametrised in term of the slip history on the fault (earthquakes, interseismic defornation, postseismic deformation….) • Dynamic model: Deformation, including slip history on faults is deduced from the rheology and boundary conditions.

12. Is this model consistent with our understanding of the mechanics of crustal deformation?What is the reason for transition to the Locked Fault one to the Creeping zone?

13. Crustal Rheology ‘brittle’ ‘ductile’ (Kohlstedt et al., 1995)

14. In all plots solid lines are linear least squares fit to the data. Dotted lines represent fit to data of the flow-law at the bottom of each plot (Mackwell et al., 1998)

15. The shear stress at frictional yield depends linearly on normal stress Static Friction is generally of the order of 0.6 for most rock types (Byerlee, 1978)

16. Condition for ‘stick-slip’ sliding Stick-slip motion requires weakening during seismic sliding, hence static friction > dynamic friction (Scholz, 1990) • unstable slip is possible if the decrease of friction is more rapid than elastic unloading during slip (‘slip weakening’) • The fault needs to restrength with time afetr slip event (‘healing’).

17. Static friction depends on hold time Dc Dynamic friction decreases with slip rate (Marone, 1998)

18. Rate-and-State Friction (Scholz, 1990) t/s=m=m*(T)+a ln(V/V*)+b ln(q/q*) dq/dt=1-Vq /Dc (Dieterich 1981; Ruina 1983) Generally a and b are of the order of~ 10-3-10-2 (e.g., Blanpied et al, 1998; Marone, 1998)

19. Rate-and-State Friction (Scholz, 1990) t/s=m=m*(T)+a ln(V/V*)+b ln(q/q*) dq/dt=1-Vq /Dc (Dieterich 1981; Ruina 1983) At steady state:qss= Dc /V mss= m*+(a-b) ln(V/V*)

20. Effect of temperature and normal stress on friction A, Dependence of (a - b) on temperature for granite . B, Dependence of (a - b) on pressure for granulated granite. This effect, due to lithification, should be augmented with temperature. Laboratory experiments show that stable frictional sliding is promoted at temperatures higher than about 300°C, and possibly at low temperatures.

21. Rate strengthening (a-b>0) : • quartzo-feldspathic rocks :T<100C or T>300C • poorly cohesive fault-gouge • Some clays at low temperature (T<100C), • serpentine (T<400C). (Marone, 1998)

22. Condition for ‘stick-slip’ Stick-slip motion requires weakening during seismic sliding, hence static friction > dynamic friction • - unstable slip is possible if the decrease of friction is more rapid than elastic unloading during slip (‘slip weakening’)

23. Condition for ‘stick-slip’ mss= m*+(a-b) ln(V/V*) • At steady state: • The system is rate-strengthening if a-b>0, only stable sliding is permitted • The system is rate-weakening if a-b<0, • - stick-slip slip is possible if the decrease of friction is more rapid than elastic unloading during slip: F/u>K, i.e. (ms-md) σn/Dc>K • - The system undergoes stable frictional sliding (conditional stability) if F/u<K, i.e. (ms-md) σn/Dc<K (Rice and Ruina 1983; Sholz, 1990)

24. Stationary State Frictional Sliding mss== t/s= m*+(a-b) ln(V/V*) (Rice and Ruina 1983) a-b < 0 slip is potentially unstable a-b > 0 stable sliding a-b Correspond to T~300 °C For Quartzo-Feldspathic rocks (Blanpied et al, 1991)

25. Tinter= 96.2 ans Seismic Cycle Modeling Maximum sliding velocity on the fault as a function of time. Slip as a function of depth. Each line represents the slip distribution at a given time. Every 5 yr in the interseismic period. For velocity change of 10% durin dynamic rupture. (Perfettini et al, 2003)

26. Slip as a function of depth over the seismic cycle of a strike–slip fault, using a frictional model containing a transition from unstable to stable friction at 11 km depth (Tse and Rice, 1981; Shloz, 1992)

27. Aseismic stable frictional becomes dominant for temperatures above ~ 300°C-400°C. (Avouac, 2003) This is consistent with laboratory experiments which show that stable frictional sliding (a-b>0) is promoted at temperatures higher than about 300°C for Quartzo-felspathic rocks.Fluids may play a role too (cf MT results). From Blanpied et al, (1991)

28. Constitutive laws used to model crustal deformation and the seismic cycle Frictional sliding (rate-and-state friction) t/s=m=m*+a ln(V/V*)+b ln(q/q*) dq/dt=1-Vq /Dc Ductile Flow dε/dt = A fH2Omσn ℮-Q/RT

29. (Cattin and Avouac, JGR, 2000) FEM code: ADELI (Hassani, Jongmans and Chery 1997) Rheology: Brittle failure (Drucker-Prager criterion) Non linear, temperature dependent creep law Surface processes: Linear diffusion + flat deposition in the foreland Boundary conditions: Hydrostatic fundation, 20 mm/yr horizontal shortening

30. Mechanical model • FEM ADELI (Hassani, Jongmans and Chery 1997)- Rheology: Coulomb brittle failure + Non linear creep law depending on local temperature. • - Surface processes: linear diffusion and flat deposition in the foreland- Boundary conditions: Hydrostatic fundation, 18mm/yr horizontal shortening (Cattin and Avouac, JGR, 2000)

31. Due to the thermally activated flow law the model predicts a localized ductile shear zone that coincides with the creeping zone of the MHT. (Cattin and Avouac, JGR, 2000)

32. 21 +/-1.5 mm/yr The effective friction on the MHT needs to be low (<0.1)

33. Modeling InterseismicDeformation • Provided that effective friction on MHT is low (<0.1), the model reconciles geodetic and holocene deformation • Seismicity falls in the zone of enhanced Coulomb stress in the interseismic period (Cattin and Avouac, 2000)

34. Modeling postseismic Deformation

35. Modeling postseismic Deformation

36. (c) Viscoelastic stress relaxation model for Chile, viscosity 2.5  1019 Pa s (Hu et al, 2004)

37. (hu et Earthquake followed by locking (Hu et al, 2004)

38. Different along-strike rupture lengths and slip magnitudes (surface velocities 35 years after an earthquake; mantle viscosity 2.5 x 1019 Pa s) (Hu et al, 2004)

39. A simple Fault Model • Locked Fault Zone • Brittle Creeping Fault Zone: • Ductile Shear Zone

40. A simplified springs and sliders model F a-b<0 a-b>0 Frictional sliding Ductile Shear F: Driving Force (assumed constant) Ffr : Frictional resistance Fh: Viscous resistance to F = Ffr + Fh F < FfrNo slip F > FfrStick-slip (Perfettini and Avouac, 2004b)

41. Stress transfer during the seismic cycle Fh >> DFfr F : Driving Force (assumed constant) DFfr : Co-seismic drop of frictional resistance Fh: Viscous resistance Two characteristic times are governing the temporal evolution of deformation - Brittle creep relaxation time tr - Maxell timeTM Fh DFfr (Perfettini and Avouac, 2004b)

42. Interseismicdisplacement at AREQ relative to stable South America is landward. The persistent seaward motion of AREQ after the earthquake is due to postseismic relaxation. The modeling suggest that may be interseismic is never really stationary (Perfettini et al, 2005) Displacement at AREQ relative to stable South America before and after the Mw 8.1, 2001, Arequipa earthquake.

43. References Cohen, S. C. (1999), Numerical models of crustal deformation in seismic zones, Adv. Geophys., 41, 134-231. Wang, K, Elastic and Viscoelastic Models of Crustal Deformation in Subduction Earthquake Cycles, In The Seismogenic Zone of Subduction Thrust Faults, edited by T. Dixon and J. C. Moore, Columbia University Press, 2007 . Cattin, R., and J. P. Avouac (2000), Modeling mountain building and the seismic cycle in the Himalaya of Nepal, Journal of Geophysical Research-Solid Earth, 105(B6), 13389-13407. Wang, K. L., J. H. He, H. Dragert, and T. S. James (2001), Three-dimensional viscoelastic interseismic deformation model for the Cascadia subduction zone, Earth Planets and Space, 53(4), 295-306. Hu, Y., K. Wang, J. He, J. Klotz, and G. Khazaradze (2004), Three-dimensional viscoelastic finite element model for postseismic deformation of the great 1960 Chile earthquake, Journal of Geophysical Research-Solid Earth, 109(B12). Perfettini, H., and J. P. Avouac (2004), Stress transfer and strain rate variations during the seismic cycle, Journal of Geophysical Research-Solid Earth, 109(B6).