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Earthquake
Social Issues
Detailed study of earthquakes gives rise to more information about societal issues (such as seismic
hazard or risk), tectonics (in the broad sense, e.g. stress fields, as well as on a smaller scale such as
in hydrocarbon reservoirs and geothermal energy plants), and the wave motion generated by the
earthquake.
� The “beach ball” diagrams of focal mechanisms can give information about the type and
orientation of earthquakes such as the tsunami triggering earthquake suffered by Sumatra.
� In the San Francisco Bay Area, there are several kilometers of separation between the San
Andreas Fault and the Hayward Fault, creating a wide rupture zone.
� The East African Rift System creates extensional stress in East Africa as well as Atlantic and
South Atlantic spreading. This system also causes motion of the Indian plate. Also note that
extension implies that the African plate must grow, so the plate geometries are changing.
Difference between seismic hazard and risk
� Seismic hazard: what is the probability of occurrence.
� Seismic risk: what damage could it do.
Earthquake Location and Focal Mechanisms
Once seismic information is recorded, two questions must be answered.
- How do we locate earthquakes?
- How do we reconstruct focal mechanisms?
A. Tectonic Frame
First, let’s get back into the tectonic frame. The equation of motion (Cauchy or Navier) is given by
2
u
i
= δ σ + f (1)
∂ t
2
j ij i
where f
i
represents the body forces such as gravity and electromagnetism due to coupling
between the seismic and electric fields. Setting the body forces to zero leads to
2
u
i
∂ t
2
j ij
In theory, we try to find the equivalent body forces that best describe the fault motion and put
1
Note 04/28/
them into equation (1). This is formally known as the “Representation Theorem” which is further
discussed in, e.g., Ahi and Richards.
B. Green’s Function
For a point source at (
x
, t
)
, the solution for the equation of motion is given by a Green’s
Function G (
x t , )
. The force can be represented as follows
f
i
(
x
, t
)
= A δ (
x − x
)
δ (
t − t
)
δ (3)
in
where A is the amplitude, (
t − t
)
is time, (
x − x
)
is position, and n is the direction.
Putting this into the equation of motion and solving for u
i
(the displacement field resulting from
wave motion due to a point source) gives the Green’s Function G ( ,
x x , , t t
)
2
2
G
in
(
x − x ′ )
(
t − t ′ )
in
c
ijkl
G
kn ⎟
(4)
∂ t ∂ x
j ⎝
x
l ⎠
Note that
∂ G
G
in
in
= 0 if x ≠ x
and t < t
(5)
∂ t
If t
= 0 , that is
f (
x
)
= B
(
t )
(
x − x
)
(
t )
i in
The solution gives the Green’s Function G (
x x , , 0 t )
. Then we integrate it over time and space
∞
x t , = dt f x , t
G x x , , 0 dV x
u ( )
∫
∫∫∫
i
(
) (
t ) ( )
n
(7)
−∞ Volume
Thus, a seismogram can be built by integrating over the Green’s Functions. For simplicity, we can
also denote equation (7) as
∞
u (
x t , )
∫
f (
x
, t
)
G
ij
(
x t , − t
, x
)
dt
(8)
i
−∞
or
2
Note 04/28/
Figure 2
Problems arise when the source is too shallow, giving a low h value. When this happens, the
travel time difference is small and makes it difficult to distinguish between the two arrivals. Using
a combination of depth phases and travel time differences can give a good estimate of the
hypocenter of the earthquake.
D. Refinement of Source Location
If we have tthe initial guess of hypocenter m = (
t , h , θ , ϕ
)
, then for the actual source m
0 0 0 0 0
T = T
(
m )
� T
(
m
0
)
+δ T (10)
obs
where δ T is the travel time residual. From travel time tomography, we have
δ T = T
obs
− T
ref
=δ T
3D structure
+δ T
Source mislocation
The linearized residual for source mislocation is
δ T = δ t + δ h + δθ + δϕ
∂ t
0
∂ h
0
0
0
(12)
(
∇′⋅ T
)
⋅δ m
where
(
)
m = t , δ h , δθ δϕ (13)
Combine this with residual from 3D structure, we have
4
Note 04/28/
m
3 D
(
A
3 D
� A
eq
)
= d (14)
m
eq ⎠
That is
Am = d (15)
The solution is
-
T T
m =
(
A A
)
A d (16)
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