The Nature and Cause of Earthquakes - KITP Online...
Transcript of The Nature and Cause of Earthquakes - KITP Online...
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The Nature and Cause of Earthquakes
• What is an earthquake?
• Why do earthquakes occur?
• Where do earthquakes occur?
• How do we represent an earthquake kinematically?
• How do we represent an earthquake dynamically?
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Most destructive 20th-21st century events:DATE LOCATION DEATHS MAG
December 16, 1920 China, Gansu 200,000 8.6May 22, 1927 China, near Xining 200,000 8.3December 25, 1932 China, Gansu 70,000 7.6July 27, 1976 China, Tangshan 255,000-655,000 7.8
September 1, 1923 Japan, Kwanto 143,000 8.3
May 30, 1935 Pakistan, Quetta 30,000-60,000 7.5June 20, 1990 Iran 50,000 7.7
October 5, 1948 USSR 110,000 7.3
December 28, 1908 Italy, Messina 70,000-100,000 7.5
May 31, 1970 Peru 66,000 7.8
December 26, 2004 Sumatra/Andaman Is. ~300,000 9.15
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August 17, 1999, Izmit, Turkey, Mw=7.4, > 10,000 deaths {New YorkTimes, 1999; USGS, 1999}
Recent destructive event:
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50,000 7.7 Landslides.Earthquake definitions:
The sudden slip on a fault (release of elastic energy), andthe resulting ground shaking and radiated seismic energy causedby the slip, … {USGS, 2002}.
Other
• Quaking and subsequent shaking of Earth with varied causes(volcanic, impact, landslides, explosions, fault motion) {NaturalDisasters, 1999}
• Sudden violent movement within the crust or upper mantle {TheSolid Earth, 1990}
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Sequence:
1) Tectonic loading of faults
2) Earthquakes
3) Seismic waves
4) Shaking (ground motion)
5) Structural failure
1995, KOBE, JAPAN
?
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Structural failure: damage orcollapse of structures (buildings,roads, dams, gas and electricallines) that lead to a loss of lifeand property.
January 17, 1995, Kobe, Japan,Mw=6.9, > 5000 deaths
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Shaking (groundmotion): groundmovement or motion ofthe earth that causesstructures to react, i.e.,that induces motion inthe structure that canlead to failure.
Shaking video
An example of shaking in southern California due to the 1999 M7.4 Izmit earthquake inTurkey. [T. Tanimoto, UCSB]
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Seismic waves: the propagation of the disturbance (energy) thatwe recognize as shaking.
Center for Advanced Studies, Research and Development in Sardinia, 2002
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Earthquake: The release of elastic energy by sudden slip on afault, and the resulting ground shaking and radiated seismic energycaused by the slip.
San Andreas M=7.75 simulation (Olsen, K. and R. Archuleta. UCSB)
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Fault: A fracture (crack) in the earth, where the two sides movepast each other and the relative motion is parallel to the fracture.
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Fault specification:
90˚ dip = vertical fault plane
0˚ strike = north parallel fault plane
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Surface trace (San Andreas, Carrizo Plain):
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Parkfield
2004 SAF Surface Fractures (red) and Other Faults (yellow)2004 SAF Surface Fractures (red) and Other Faults (yellow)
Mike Rymer, USGS, 2005
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Earthquake (initial slip) locations:
If one side of the fault is removed, the footwall is exposed showing therupture covers the fault surface and is not simply some point on the surfaceof the earth.
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Fault types:
1) Dip-slip - major offset in the dip (vertical) direction
a) Normal - hanging wall moves down
b) Reverse - hanging wall moves up
2) Strike-slip - major offset in the strike (horizontal) direction
a) Left-lateral
b) Right lateral
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Movies: Styles of FaultingStrike-slip Dip-Slip: Reverse
Dip-Slip: Normal
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1983 Borah Peak Earthquake, Idaho
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Thrust (reverse) faulting
1964 Alaska, PrinceEdward Island
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Strike-Slip Faulting 1979 Imperial Valley Earthquake
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Sudden slip by elastic rebound theory:
1) Stresses (force/area) are applied to a fault.
2) Strain (deformation) accumulates in the vicinity of friction-locked faults.
3) Strain accumulation reaches a threshold and fault slips suddenly
4) Rupture (slip) continues over some portion of the fault.
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1) Tectonic loading of faults
2) Earthquakes
a) Fault definition
b) Fault specification
c) Fault types
d) Sudden fault slip
3) Seismic waves
4) Shaking (ground motion)
5) Structural Response (sometimes failure)
Sequence:
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Tectonic plates:
USGS
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Tectonic loading of faults:
Plate tectonics: A theory of global tectonics in which thelithosphere is divided into a number of plates that act like rigidbodies and that interact with one another at their boundariescausing earthquakes, volcanism and deformation.
Tectonics: Study of the deformational features and movement[and their relations and historical evolution] of the outer part ofthe Earth.
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Earthquakes and plate boundaries:
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1) Stresses (force/area) are applied to a fault.
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2) Strain (deformation) accumulates in the vicinity offriction-locked faults.
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3) Strain accumulation reaches a threshold and fault slipssuddenly.
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4) Rupture (slip) continues over some portion of the fault.
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Kinematic Model
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Finite Fault--Kinematic (Haskell, 1966)
• Fault
Geometry:
Length, Width
• Slip
• Rise Time
• Rupture
Velocity
Slip
Ra
teS
lip
Time
Time
Rise Time
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Imperial Valley Kinematic Parameters
0
180
Cm
From Archuleta, 1984, JGR
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Behavior of Shear Stress at a Point on the Fault
TimeShear
Str
ess a
t a P
oin
t on t
he F
ault
Yield Stress
Initial Stress
Sliding Friction Stress
Final Stress
0 1 0 f
0
1
f
y
S=( y 0)/( 0 f)=Strength Excess/Stress Drop
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Dieterich’s Experiments
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Anelastic Behavior at the Crack Tip to
Eliminate the Stress SingularityStress
Dislocation
dc
f
o
y
Crack
Ida, 1972
1
1
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Madariaga, Olsen, Archuleta,
1998
Friction drops rapidly
from upper limit to
sliding friction over a
characteristic distance
Do.
Region where the sliding is at a nearly
constant value of friction.
Region where the friction
rises and the slip rate
rapidly goes to zero,
locking the fault.
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Static Stress Drop and Strength Excess
From Bouchon, 1997, JGR
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Snapshots of
Fault Plane
Showing
Evolution of
1) Stress
Drop
2) Slip Rate
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Imperial Valley Dynamic Rupture
Favreau and Archuleta, Geophys. Res. Lttr., 2003
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Seismic Energy Diagram: Slip WeakeningS
he
ar
Str
ess
y
o
f
Slipdc
Area of Triangle = Fracture
Energy
Area in Orange = Available Radiated Energy ( for f = 1)
D
Ida, 1972
Area of Trapezoid is Potential
EnergyArea of Rectangle is Energy Lost to
Heat
0
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Parkfield – bilateral 1D velocity model
SW (fast) NE (slow)SW (fast) NE (slow)
Velo
city (k
m/s)
2.0 km/s <VP< 8.0 km/s 1.1 km/s <VS< 4.5 km/s
Fault dip = 89o
Fault buried 0.5 km below the surface
Dip = 89o
1D velocity model interpolated from the 3D velocity model of Thurber et al. (2003)
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0 10 20 -20
0
20 0.127
EW
C3W
0 10 20 -20
0
20 0.290
NS
0 10 20 -5
0
5 0.945
UD
0 10 20 -20
0
20 0.156C4W
0 10 20 -10
0
10 0.244
0 10 20 -5
0
5 0.932
0 10 20 -10
0
10 0.312FZ4
0 10 20 -5
0
5 0.410
0 10 20 -5
0
5 0.907
0 10 20 -20
0
20 0.134FZ6
0 10 20 -10
0
10 0.182
0 10 20 -5
0
5 1.006
0 10 20 -20
0
20 0.124FZ9
0 10 20 -10
0
10 0.140
0 10 20 -2
0
2 0.870
0 10 20 -5
0
5 0.206GH2W
0 10 20 -5
0
5 0.363
0 10 20 -2
0
2 0.711
0 10 20 -10
0
10 0.187GH3W
0 10 20 -10
0
10 0.216
0 10 20 -2
0
2 0.697
0 10 20 -5
0
5 0.475GH5W
0 10 20 -5
0
5 0.343
0 10 20 -2
0
2 0.844
0 10 20 -5
0
5 0.220VC4W
0 10 20 -5
0
5 0.194
0 10 20 -2
0
2 0.565
0 10 20 -2
0
2 0.044WFU
0 10 20 -5
0
5 0.044
0 10 20 -2
0
2 0.627
Time (s)
Particle Velocity (cm/s)
Inversion ResultsBlue: DataBlue: Data
Red: SyntheticRed: Synthetic
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Kinematic Parameters
from One Inversion of
20 3-Component Stations
Mo: 1.0 x 1025 dyne-cm
Avg. Rupture Velocity: 3.3 km/s
Avg. Rake: 165˚
Avg. Misfit in Inversion: ~0.22
Avg. Misfit in Prediction: ~0.60
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Dynamic Energy BalanceFault Representation
Surface Representation
WqS
= ij ij0( )0
t1S
˙ u in jdtdS
WeS
= 12 ij
1ij ij
0( )ui1n jdS
S
Eq = WqS We
S
Total work done by seismic waves:
Static work:
Radiated energy:
Energy loss (fractureenergy+frictional heat)
Potential energy change
Eq = Wtotal Wstatic = ˙ D (t)d dtt
12
( 0 1)d
Eq = [ 0 (t)] ˙ D (t)d dtt
12
( 0 1)d
Eq =12
( 0+
1)Dd ˙ (t)D(t)d dtt
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Energy Densities on the Fault
Dc uu1
1d
s
0
we
y( u)
1d
s
0
Dc uu1
wf
wr
y( u)
eq we
wf
wr
= - -
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State of Stress in the Earth0 100 200 300 400 500
0
5
10
15
20
25
Shear Strength (MPa)
Friction Law μ = 0.75
Plastic Flow Law, wet quartzite20˚C km-1g = 10-12 s-1
Modified from Scholz (2002)
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Guattieri and Spudich, 200
Model A
slip
Sh
ea
r str
ess
0.3 m
Model B
slip
Sh
ea
r str
ess
1.0 m