Transcript ppt

Earthquake interaction
• The domino effect
• Stress transfer and the Coulomb Failure Function
• Aftershocks
• Dynamic triggering
• Volcano-seismic coupling
Earthquake interaction: The domino effect
Example from California:
Figure from www.earthquakecountry.info
Earthquake interaction: The domino effect
Example from the North Anatolia Fault (NAF):
Figure from Stein et al., 1997
Earthquake interaction: The Coulomb Failure Function
Slip on faults modifies the stress field:
Animation by USGS
Waveforms of the
April 4, 2010, Mw
7.2 El MayorCucapah
earthquake
recorded at P494.
Earthquake interaction: The Coulomb Failure Function
A function that measures the enhancement of the failure on a
given plane due to a stress perturbation is the Coulomb Failure
Function (CFF):
where:
S is the shear stress (- positive in the direction of slip)
N is the normal stress (- positive in compression)
M is the coefficient of friction
Failure on the plane in question is enhanced if CFF is
positive, and is delayed if it is negative.
Earthquake interaction: The Coulomb Failure Function
The figures above show the change in the fault-parallel shear
stress and fault-perpendicular normal stress, due to right-lateral
slip along a dislocation embedded in an infinite elastic medium
Earthquake interaction: The Coulomb Failure Function
Earthquake interaction: The Coulomb Failure Function
The area affected by the stress perturbation scales with the
rupture dimensions.
The change in CFF due to
the eight largest
earthquakes of the 20th
century.
Alaska, 1964, Mw9.2
Chile, 1969, Mw9.5
Figure from: legacy.ingv.it/~roma/attivita/fisicainterno/modelli/struttureattive
Earthquake interaction: The Coulomb Failure Function
Example from NAF
Animation by USGS
Earthquake interaction: Stress shadows
The 1906 Great California stress shadow:
Stein, 2002
So the CFF concept works not only for positive, but also for
negative stress change.
Earthquake interaction: Multiple stress transfers - The Landers
and Hector Mine example
Maps of static stress changes
suggest that the Landers
earthquake did not increase the
static stress at the site of the Hector
Mine rupture, and that Hector Mine
ruptured within a “stress shadow”.
Kilb, 2003
Earthquake interaction: Multiple stress transfers - The Landers
and Hector Mine example
This map shows the
change in CFF caused
by the Landers quake on
optimally oriented planes
at 6km depth. The arrows
point to the northern and
southern ends of the
mapped surface rupture.
Figure downloaded from
www.seismo.unr.edu/htdocs/WGB/Recent.old/HectorMine
Earthquake interaction: Multiple stress transfers - The Landers
and Hector Mine example
• Most Landers aftershocks in the
rupture region of the Hector Mine
were not directly triggered by the
Landers quake, but are secondary
aftershocks triggered by the M 5.4
Pisgah aftershock.
• The Hector Mine quake is,
therefore, likely to be an aftershock
of the Pisgah aftershock and its
aftershocks.
Felzer et al., 2002
Earthquake interaction: Aftershock triggering
Maps of CFF calculated following major earthquakes show a
strong tendency for aftershocks to occur in regions of positive
CFF.
The Landers earthquake (CA):
King and Cocco (2000);
Stein et al., 1992.
Earthquake interaction: Aftershock triggering
The Homestead earthquake (CA):
King and Cocco (2000).
Earthquake interaction: Remote aftershock triggering
N˙ (Landers + 10 days) - N˙ (Landers - 100 days)
N˙ (1985 - 2002)
N˙ (HM + 10 days) - N˙ (HM - 100 days)
N˙ (1985 - 2002)
Earthquake interaction: Remote aftershock triggering
While seismicity rate
increase in the north
following the Landers
quake lasted several
months, Hector Mine
aftershock activity in
the south lasted only up
to 10 days.
Earthquake interaction: Remote aftershock triggering
The Mw7.4 Izmit (Turkey):
Mw5.8
Two weeks later
N˙ (Izmit + 10 days) - N˙ (Izmit - 100 days)
N˙ (1985 - 2002)
Earthquake interaction: Remote aftershock triggering
The decay of M7.4 Izmit
aftershocks throughout Greece
is very similar to the decay of
M5.8 Athens aftershocks in
Athens area (just multiply the
vertical axis by 2).
Earthquake interaction: Dynamic triggering
• The magnitude of static
stress changes decay as
disatnce-3.
• The magnitude of the peak
dynamic stress changes
decay as distance-1.
• At great distances from the
rupture, the peak dynamic
stresses are much larger
than the static stresss.
Figure from Kilb et al., 2000
Earthquake interaction: Remote aftershock triggering
From Shearer’s textbook
Earthquake interaction: Dynamic triggering
Instantaneous triggering
Time
No triggering
Time
Earthquake interaction: Dynamic triggering
Indeed, distant aftershocks are observed during the passage of
the seismic waves emitted from the mainshock rupture.
Izmit aftershocks in Greece.
Brodsky et al., 2000
Earthquake interaction: Dynamic triggering
Fig. from Stein and Wyssion
Earthquake interaction: Dynamic triggering
• Dynamic stress changes trigger aftershocks that rupture during
the passage of the seismic waves.
• But the vast majority aftershocks occur during the days, weeks
and months after the mainshock.
• Dynamic stress changes cannot trigger “delayed aftershocks”,
i.e. those aftreshocks that rupture long after the passage of the
seismic waves emitted by the mainshock.
• It is, therefore, unclear what gives rise to delayed aftershocks in
regions that are located very far from the mainshock.
Earthquake interaction: The role of multiple interactions
 Rate- and state-dependent friction (Dieterich-Ruina).
 Spatially discrete, i.e. L>>Lc.
 Quasi-static or quasi-dynamic.
 Periodic boundaries.
Earthquake interaction: The role of multiple interactions
Applications of uniform stress
steps:
•Aftershock duration, the
magnitude of the seismicity rate
change and the decay rate are in
good agreement with Dieterich’s
[1994] prediction.
Earthquake interaction: The role of multiple interactions
Application of non-uniform stress change:
• Aftershocks in Zone-2 are aftershocks of
the Zone-1 shocks.
• The area experiencing seismicity rate
change is much larger than that
subjected to a stress change.
So multiple stress transfers may
explain delay remote aftershocks
Earthquake interaction: Volcano-seismic coupling - the Apennines
and Vesuvius example
How normal faulting in the Apennines may promote diking and
volcanic eruptions in the Vesuvius magmatic system, and vice
versa.
Nostro et al. (1998)
Earthquake interaction: Volcano-seismic coupling - the Apennines
and Vesuvius example
Coulomb Failure Function calculations
Stress on a dike striking
parallel to the
Apennines
Nostro et al. (1998)
Stress on a dike striking
Perpendicular to the
Apennines
Pressure change on a
spherical magma
chamber
Earthquake interaction: Volcano-seismic coupling - the Apennines
and Vesuvius example
Volcano-seismic coupling?
Nostro et al. (1998)
Further reading:
• Scholz, C. H., The mechanics of earthquakes and faulting, NewYork: Cambridge Univ. Press., 439 p., 1990.
• Harris, R. A., Introduction to special section: Stress triggers,
stress shadows, and implications for seismic hazard, J. Geophys.
Res., 103, 24,347-24,358, 1998.
• Freed, A. M., Earthquake triggering by static, dynamic and
postseismic stress transfer, Annu. Rev. Earth Planet. Sci., 33, 335367, 2005.