the use of earthquake rate changes as a stress meter at kilauea volcano nature, v. 408, 2000 by j....
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![Page 1: The use of earthquake rate changes as a stress meter at Kilauea volcano Nature, V. 408, 2000 By J. Dietrich, V. Cayol, and P. Okubo Presented by Celia](https://reader034.vdocument.in/reader034/viewer/2022051401/56649e315503460f94b22a91/html5/thumbnails/1.jpg)
The use of earthquake rate changes as a stress meter at Kilauea volcano
Nature, V. 408, 2000
By J. Dietrich, V. Cayol, and P. Okubo
Presented by Celia Schiffman
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Do changes in stress correlate with changes in earthquake
rates?• Stress changes and EQ rates are not linearly
correlated• EQ nucleation process is dependent on time and
stress (lab. observations)• Estimating stresses that drive EQ’s versus stress
changes resulting from EQ’s.• Kilauea:
– Frequent stressing events– Independent observations of deformation– High rates of seismic activity– Changes in seismicity/eruptions/subsurface magma
movement– Rift-zone magmatic expansion/detachment faulting
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Formulas
R r
Sr
1) R r
Ý S rwhere d
1
Adt dS
state var iable [time /stress]
R earthquake rate (M1 M2)
r ss eq rate at Ý S rA dimensionless fault constitutive param (0.005 0.015)
normal stress min us pore fluid pressure, assume small stress changes
2) S S mod ified CS func
shear stress (pos in slip direction )
coeff of fault friction
constitutive param 0.25
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Formulas
Stress step --> characteristic aftershock sequence (i.e. immediate jump in seismicity then decay according to Omori’s decay law [1/t])
1) R r
Ý S rwhere d
1
Adt dS
where ta A
Ý S
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Two methods to estimate stress change from EQ rates
1) Stress as a function of time in a specific volume
-Calculate time series at grid points from earthquake rate data
-Calculate stress changes over succesive time intervals using stress steps at the midpoint of each time interval
(t) r
R(t) Ý S rwhere R(t) is observed, Ý S r is estimated
and r( Ý S r) from 1976 2000
Ý S Ata
d dt
A S
A
S A
dt
A d
S A dt AdAi
i1
S A lni
t
2Ai1
t
2A
S
time
t
(t1,1)
(t2,2)
S
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Two methods to estimate stress change from EQ
rates2) Spatial distribution of stress changes for a stress event (EQ or intrusion)
-Use eq 1 to solve for constant stressing at Sr, take a stress step (corresponding to the stress event), then constant stressing at Sr again.
S
Ý S r exp(N2Ý S rt1
N1A ) 1
Ý S r exp(Ý S rt2
A ) 1
where N1 # eq's in t1N2 # eq's in t2
S depends on fault orientation and slip direction
-Eq counts are made for subregions sorted byfault orientation-6-13 km depths-Each volume needs at least 8 EQ’s-Grid nodes spaced 1 km apart
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Timeline• Pre 1975:
– Eruptive activity• 1975:
– M7.2 EQ• 1975-1983:
– Intrusion (1977)– Rapid deformation (up to 25 cm/yr extension)– Intense seismicity– Aseismic creep on detachment– Rift opening at 40 cm/yr
• 1979-1983:
– 5 fold slowing of stressing rates• 1983:
– Eruption• Post 1983:
– Nearly continuous rift eruption– Deformation decreased to 4 cm/yr
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Location
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Observations
Deformation data sets
Number of earthquakes
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-Eq rates are low-pass filtered-Assume Eq’s occur on faults that are optimally oriented in the stress field
-Artifacts from random fluctuations in EQ rate and possiblecatalog inconsistencies during swarm events-Slowing of stressing rates from 1981-83 (0.3->0.15)Next: Compare to BEM’s constructed from independent estimates of stress changes
Calculate stress changes based on eq’s
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Model variables: depth, height, width, dip and opening of dikeDip and depth of detachment faultWidth of creeping portion of fault
Outputs:Predicted surface deformationsStress changes
Pick best fitting values for variablesbased on deformation data
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Pre-1983 eruption
Post-1983 eruption
Boundary Element Models
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Statistics:Slope=1.1Correlation=0.8
Problems•Non-linear relationship not clearly demonstrated•Is it really necessary?•Would a linear fit work just aswell?•Need geodetic data (GPS) to better constrainchanges in stress to see if step-function, or linear