fig. 8.00 earthquakes and earthquake hazards. 3 seismic waves allow us to look inside the earth
TRANSCRIPT
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Fig. 8.00
Earthquakes and Earthquake Hazards
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Seismic waves allow us to look inside the Earth
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€
Vp =k + 4 3μ
ρ
Vs =μ
ρ
κ = compressibility
μ = rigidity
ρ = density
Seismic Waves
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QuickTime™ and aGIF decompressor
are needed to see this picture.
www.eas.purdue.edu/~braile
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www.eas.purdue.edu/~braile
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www.eas.purdue.edu/~braile
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www.eas.purdue.edu/~braile
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Fig. 8.12ab
W. W. Norton
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Fig. 8.13ab
W. W. Norton
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Fig. 8.13c
W. W. Norton
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Fig. 8.15
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Seismic Refraction
i’
i
sin(i)
sin(i’)=
Velocity of AVelocity of B
A
B
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Refraction
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Seismic wave tomography — a CAT-scan of the interior
Colors are seismic wave velocity anomalies
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Red = slow (hot)
Blue = fast (cold)
Here is a slice through North America showing the now-subducted Farallon Plate, sinking to the bottom of the mantle.
Heating reduces rigidity more than it reduces density, so hotter material have slower seismic velocities
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How Faults Work — the Mechanics of Earthquakes
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Static Friction with a spring
Fn
Fs=kx
At time of sliding τ =μs σ , where μs is the static coefficient of friction
σ = Fn/A(A= area of base)
τ = Fs/A
Why Earthquakes (stick-slip behavior)?
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Fn
Fs=kx
Fs
Displacement
If friction was this simple — and if the applied forces, coming from plate motions, were constant — would we have stick-slip behavior?
μs
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Of course, friction is NOT so simple — the coefficient of friction changes once sliding begins, and if μd < μs, then we should see the idealized stick-slip behavior
slip
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τ
Displacement
μs σ
μd σ
slope is -k (spring constant)
Idealized Stick-Slip Behavior
μs = μstatic
μd = μdynamic
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EQ Slip Model
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As the rupture grows, more energy is released and a larger magnitude earthquake results. If a big segment of the fault is right near the limit, a small rupture can take off and grow into a huge rupture and a huge earthquake
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τ
Displacement
μs σ
μd σ
Idealized Stick-Slip Behavior
This is equivalent to the “re-loading” timeif we assume that the tectonic driving forces are applied at a steady rate
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Time
Dis
pla
cem
en
t
Plate tectonic rate and friction along fault determine recurrence time and average size of earthquakes
Earthquake event
Time between earthquake — re-loading time
plate tecto
nic rate
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Time
Dis
pla
cem
en
t
Same plate tectonic rate, but low friction (weaker fault plane), so shorter recurrence time and smaller earthquakes
Earthquake event
Time between earthquake
plate tecto
nic rate
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rocks in the circles were formerly right next to each other
The San Andreas Fault is the plate boundary between NAM and PAC
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4 cm/yr x 100 yr = 4 m (avg slip for M8 EQ)
Slip on the fault occurs in small segments, but over time, every part of the fault has to accommodate the 4 cm/yr plate tectonic rate
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Normal Fault Surface Scarp
Borah Peak, Idaho M 7.3 October 28, 1983
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1964 Alaskan Earthquake (M~9.2)
This side moved up about 6 m
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M~8