1. Geology 5640/6640 Introduction to Seismology 25 Feb 2015 © A.R. Lowry 2015 Last time: Seismic Source Modeling For an earthquake, the f(t) in the source term of the wave equation: is a (tensor) moment rate of energy release: (& moment is M =  sA !) The moment rate function can be used to solve for amount of slip, direction of slip, and speed of rupture propagation on a fault. This in turn tells us something about history of fault slip (including recent evolution and stress relieved in past earthquakes) & frictional stability. Read for Fri 27 Feb: S&W 75-86 (§2.6)

2. Source Seismology 2011 Christchurch earthquake, M6.3, after a larger M7.0 eq further west in 2010… Difference is proximity… 2 injured NZ $4B 2010 M7.0 2011 M6.3 185 dead NZ $15B

3. Can use this to get other interesting pieces of information about the earthquake rupture process…

4. … Including our growing recognition that many large earthquakes involve complex rupture simultaneously on several faults that may have completely different dip and orientation.* *Lesson for Utah! Ya think future Wasatch rupture won’t cross segment boundaries? Ya got another think comin’. Hayes et al., Nat. Geosci., 2010 Crone et al., BSSA, 2004 2010 M7.0 Haiti 2002 M7.9 Denali

5. Seismic Wave Energy Partitioning With Snell’s Law in our tool-belt, we’re ready to consider what happens to seismic amplitudes when an incoming wave arrives at a change in properties (and hence, conversions occur). One obvious thing that has to happen is conservation of energy : i.e., reflected energy + transmitted energy = energy of the incoming wave As you might expect, energy is related to amplitude of the wave. incoming P A 

6. Impedance Contrast: Thus far we’ve focused much of the discussion on concepts related to velocity & travel-time, but seismic waves also have amplitude, A, of the particle displacements: Amplitudes of reflections & refractions are determined by energy partitioning at the boundary. A normally-incident (  = 0 ) P-wave with amplitude A i produces a reflected P with amplitude: incoming P A  ( reflection coefficient ) and a refracted P: where Z i =  i V i is the impedance in layer i. ( transmission coefficient )

7. The energy E in a wave is directly proportional to the amplitude A, and for this example, sign (i.e. propagation direction) matters. We’ll use the sign of the z -component (positive-down) of propagation. Then we have: Displacement must be continuous at the boundary so: A i + A rfl = A rfr And: 1 + R = T Note however for the P-wave depicted here, this applies only to the case where  i = 0° … ( Why? ) incoming P A 