324l8 sp

Slide1: 

8: EARTHQUAKE SOURCE PARAMETERS Magnitude, fault area, fault slip, stress drop, energy release “the big one”

Slide2: 

EARTHQUAKE MAGNITUDE Earliest measure of earthquake size Dimensionless number measured various ways, including ML local magnitude mb body wave magnitude Ms surface wave magnitude Mw moment magnitude Easy to measure Empirical - except for Mw, no direct tie to physics of faulting Note; not dimensionally correct

Slide7: 

COMPARE EARTHQUAKES USING SEISMIC MOMENT M0 Magnitudes, moments (dyn-cm), fault areas, and fault slips for several earthquakes Alaska & San Francisco differ much more than Ms implies M0 more useful measure Units: dyne-cm or Nt-M Directly tied to fault physics Doesn’t saturate Stein & Wysession, 2003

Slide8: 

EARTHQUAKE SOURCE PARAMETER ESTIMATES HAVE CONSIDERABLE UNCERTAINTIES FOR SEVERAL REASONS: - Uncertainties due to earth's variability and deviations from the mathematical simplifications used. Even with high-quality modern data, seismic moment estimates for the Loma Prieta earthquake vary by about 25%, and Ms values vary by about 0.2 units. - Uncertainties for historic earthquakes are large. Fault length estimates for the San Francisco earthquake vary from 300-500 km, Ms was estimated at 8.3 but now thought to be ~7.8, and fault width is essentially unknown and inferred from the depths of more recent earthquakes and geodetic data. - Different techniques (body waves, surface waves, geodesy, geology) can yield different estimates. - Fault dimensions and dislocations shown are average values for quantities that can vary significantly along the fault Hence different studies yield varying and sometimes inconsistent values. Even so, data are sufficient to show effects of interest.

Slide9: 

Moment magnitude Mw Magnitudes saturate: No matter how big the earthquake mb never exceeds ~6.4 Ms never exceeds ~8.4 Mw defined from moment so never saturates

Slide10: 

TIME DURATION = rupture time T R needed to propagate along fault * rise time TD for full slip at any point TR = fault length / rupture velocity SOURCE PULSE FROM EARTHQUAKE

Slide11: 

SPECTRUM OF SOURCE TIME FUNCTION

Slide12: 

SOURCE SPECTRUM is flat and equal to seismic moment at periods longer than corner frequency 2/TR Decays below corner frequency Corner frequency shifts to left (lower frequency) for larger earthquakes with longer faults HIGH LOW Seismic moment

Slide13: 

DIFFERENT MAGNITUDES REFLECT ENERGY RELEASE AT DIFFERENT PERIODS 1 s - Body wave magnitude mb 20 s - Surface wave magnitude Ms Long period - moment magnitude Mw derived from moment M0 Geller, 1976

Slide14: 

DIFFERENT MAGNITUDE SCALES REFLECT AMPLITUDE AT DIFFERENT PERIODS 20 s 1 s Body & surface wave magnitudes saturate - remain constant once earthquake exceeds a certain size - because added energy release in very large earthquakes is at periods > 20 s No matter how big an earthquake is, body and surface wave magnitudes do not exceed ~ 6.5 and 8.4, respectively. For very large earthquakes only low period moment magnitude reflects earthquake’s size. This issue is crucial for tsunami warning because long periods excite tsunami, but are harder to study in real time

Slide15: 

E. Okal

Slide16: 

SCALING RELATIONS BETWEEN SOURCE PARAMETERS

Slide18: 

THREE EARTHQUAKES IN NORTH AMERICA - PACIFIC PLATE BOUNDARY ZONE Tectonic setting affects earthquake size San Fernando earthquake on buried thrust fault in the Los Angeles area, similar to Northridge earthquake. Short faults are part of an oblique trend in the boundary zone, so fault areas are roughly rectangular. The down-dip width seems controlled by the fact that rocks deeper than ~20 km are weak and undergo stable sliding rather than accumulate strain for future earthquakes. San Francisco earthquake ruptured a long segment of the San Andreas with significantly larger slip, but because the fault is vertical, still had a narrow width. This earthquake illustrates approximately the maximum size of continental transform earthquakes. Alaska earthquake had much larger rupture area because it occurred on shallow-dipping subduction thrust interface. The larger fault dimensions give rise to greater slip, so the combined effects of larger fault area and more slip cause largest earthquakes to occur at subduction zones rather than transforms. Stein & Wysession, 2003

Slide19: 

STRAIN & STRESS CHANGES

Slide20: 

EARTHQUAKE STRESS DROPS TYPICALLY 10s TO 100s OF BARS Estimate from fault area if known Kanamori, 1970

Slide21: 

SPECTRAL CORNER FREQUENCY APPROACH

Slide22: 

Problem: for shallow earthquakes P, pP, and sP often overlap, yielding a combined spectrum quite different from the source pulse. Spectra differ between stations due to the variation in amplitude between direct and reflected arrivals, and cannot be used to corner frequencies or seismic moment. Difficulty can be addressed by modeling the body waves, including the free surface reflections, and estimating the source time function duration by matching the observed waveforms. Given a duration estimate and an assumed fault geometry, the fault length and stress drop are estimated as in corner frequency analysis.

Slide23: 

ESTIMATING STRESS DROP FROM BODY WAVE MODELING -- HARDER Stein and Kroeger, 1980 Inferring source dimension from time function requires assuming rupture velocity & fault geometry Estimated stress drop ~1 / L3 , so uncertainty in fault dimension causes large uncertainty in ∆ Small differences in time function duration correspond to larger differences in stress drop, even for assumed rupture velocity & fault geometry

Slide24: 

INTRAPLATE EARTHQUAKES THOUGHT TO HAVE HIGHER STRESS DROP (?) 4.6-11 (the slope is 3/2)

Slide25: 

IF STRESS DROP IN EARTHQUAKES IS APPROX IMATELY CONSTANT LONGER FAULTS (L LARGER) HAVE LARGER SLIP D

Slide26: 

IF STRESS DROP IN EARTHQUAKES IS APPROX IMATELY CONSTANT LINEAR DIMENSION3 OR FAULT AREA3/2 INCREASES WITH MOMENT M0

Slide27: 

LARGER EARTHQUAKES GENERALLY HAVE LONGER FAULTS AND LARGER SLIP M7, ~ 100 km long, 1 m slip; M6, ~ 10 km long, ~ 20 cm slip Important for tectonics, earthquake source physics, hazard estimation Wells and Coppersmith, 1994

Slide28: 

Compared to ridge earthquakes, transform earthquakes often have large Ms relative to mb and large Mw relative to Ms suggesting that seismic wave energy is relatively greater at longer periods. Earthquakes that preferentially radiate at longer periods are called "slow" earthquakes. Underlying physics unclear SLOW EARTHQUAKES Stein and Pelayo, 1991

Slide29: 

For a given moment and fault shape, lower stress drop corresponds to larger fault dimensions, and hence longer time functions and smaller corner frequencies. Given two earthquakes with the same rupture velocity, one with lower stress drop will have less high frequency radiation, and thus lower Ms and mb. Similar effects can result from a slower rupture velocity, which also gives a longer time function for a given fault dimension.

Slide30: 

ENERGY RADIATED BY EARTHQUAKE

Slide31: 

ENERGY & MAGNITUDE 5

Slide32: 

Earthquakes of a given magnitude are ~10 times less frequent than those one magnitude smaller. An M7 earthquake occurs approximately monthly, and an earthquake of M> 6 about every three days. Hence although earthquake predictor I. Browning claimed to have predicted the 1989 Loma Prieta earthquake, he said that near a date there would be an M6 earthquake somewhere, a prediction virtually guaranteed to be true. Magnitude is proportional to the logarithm of the energy released, so most energy released seismically is in the largest earthquakes. An M 8.5 event releases more energy than all other earthquakes in a year combined. Hence the hazard from earthquakes is due primarily to large (typically magnitude > 6.5) earthquakes.

Slide33: 

WHY? Only a small fraction of stress released ? Lab values apply to contact area, only a fraction of total fault surface ? -Lab values don’t scale correctly ?