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Subduction Zone Geodynamics:
Walking the Maze of Coupling and Decoupling
Kelin Wang
Pacific Geoscience Centre, Geological Survey of Canada
Subduction Zone Geodynamics:
Walking the Maze of Coupling and Decoupling
Coupling or decoupling
• Velocity continuous or discontinuous (long-term)
• Seismic or aseismic
• Locked or creeping (short-term)
• Strong or weak interface
~ 10
0 km
• Low seismic attenuation• Low Vp/Vs• Serpentinization• Stagnant
• High attenuation• High Vp/Vs• Melting• Vigorous wedge flow
Cold Forearc Hot Arc, Back Arc
70 ~
80 km
Blue: Basaltic crust
Purple:Serpentine stability
Basalt to eclogite ~ 40-50 km depthFeeble arc volcanismSerpentinized mantle wedge cornerIntraslab earthquakes to ~90 km depth
Basalt to eclogite ~ 100-140 kmActive arc volcanismHigh-velocity wedge cornerEarthquakes to hundreds of km
N Cascadia NE Japan
Kirby et al., 1996; van Keken et al., 2002; Wada and Wang, 2009; Syracuse et al., 2010
End-member warm-slab and cold-slab subduction zones
Survival depth of basaltic crust (blue diamonds)
anddepth range of intraslab
earthquakes (purple)
Model-predicted peak dehydration depth (blue)
andserpentine stability in
subducting slab (purple)
Wada and Wang, 2009
Warm Cold
Questions:
• What controls the abrupt transition from decoupling to coupling?• What is the role of petrology, fluids, and rheology?
?
~ 10
0 km
70 ~
80 km
Seismogenic zone(stick-slip,
velocity-weakening, “seismically coupled”)
For coseismic deformation (a few minutes), this is all elastic.
Blue: Basaltic crust
Purple:Serpentine stability
N Cascadia NE Japan
• Temperature plays a role but perhaps not via a single critical value• Continental Moho seems to be a limit, but there are counter examples:
Many events in NE Japan, 2004 Sumatra (Klingelhoefer et al., 2010)
End-member warm-slab and cold-slab subduction zones
Seismogenic zone
?
Questions:
• What determines the downdip limit of seismic rupture?• What is the frictional behavior of the slab – mantle wedge interface?
Locked zone
• Interseismic deformation changes with time and therefore is not a mirror image of coseismic deformation.
• Locked zone (future rupture zone) cannot be determined by inverting interseismic geodetic data using an elastic model.
coastline coastline
Interseismic Coseismic
Rupture
Stress relaxation
Stress relaxation
Afterslip
Locking
Three primary processes after an earthquake: afterslip, viscoelastic stress relaxation, and fault locking.
Sumatra: A few years after a great earthquake:
All sites move seaward
Courtesy Kelly Grijalva and Roland Burgmann
Alaska and Chile: ~ 40 years after a great earthquake:Opposing motion of coastal and inland sites
M = 9.2 M = 9.2 19641964
Freymueller et al. (2009)
M = 9.5 M = 9.5 19601960
Wang et al. (2007)
Inter-seismic 2 (Cascadia)
Inter-seismic 1(Alaska, Chile)
Co-seismic
Coast line
Coast line
Post-seismic (Sumatra)
Questions:• What do interseismic deformation observations tell us about
fault friction, rock rheology, and state of locking? • What can we learn by observing subduction zones presently at
different stages of the earthquake cycle?
Locked zone
?
GPS displacements and slip distribution on subduction interface determined by inverting the GPS data.
Northern Cascadia ETS event of May 2008
Tremor located by Kao (white) and Wech (gray)
Comparison with a worst-case scenario of megathrust rupture
(Ichinose et al., 2003)
(Baba and Cummins, 2005)
(Kikuchi and Yamanaka, 2001)
(Sagiya and Thatcher, 1999)
Including afterslip
19461944
1944
1944
19461944
Non-volcanic tremor
Survival depth of basaltic oceanic crust (blue)
anddepth range of intraslab
earthquakes (purple)
Model-predicted peak dehydration depth (blue)
andserpentine stability in
subducting slab (purple)
Wada and Wang, 2009
Nan
kai
Mex
ico
Ala
ska
Cos
ta R
ica
Warm Cold
Blue: Basaltic crust
Purple:Serpentine stability
N Cascadia NE Japan
ETS at mantle wedge corner
No ETS has been reported
End-member warm-slab and cold-slab subduction zones
In addition:• Other types of slow slip events: long- and short-duration slow slip
without tremor, very-low-frequency earthquakes in ETS zone … …• Vp/Vs anomaly associated with ETS (fluid?)• Mike Brudzinski will provide other details this afternoon
ETS
Seismogenic zone
Questions:• What is the relation between the earthquake cycle, ETS, and
other slow slip phenomena? • What are the thermally controlled petrologic and hydrologic
conditions of ETS?
b 0.04
b -0.01
Average stress
~ 15 MPa
Stress dropa few MPa
coastlineInterseismic
coastlineCoseismic
b > 0Stress
increasea few MPa
Co-seismic
Post-seismic
Stress increase; resisting slip
Rupture;Stress drop
Stress decrease
Locked;Stress increase
ClassicalCoulomb Wedge
DynamicCoulomb Wedge
Updip zone Seismogenic zone
Understanding how the prism is made … …
Nankai
Moore et al., 2007
(based on von Huene et al. (2004)
Costa Rica
Ranero et al., 2007
Relation between seismogenic zone and prism structure … …
Inter-seismic 2 (Cascadia)
Inter-seismic 1(Alaska, Chile)
Co-seismic
Coast line
Post-seismic (Sumatra)
?
?
?
?
How the leading edge behaves in earthquake cycles … …
Hsu et al. (2006)
2005 Nias-Simeulue earthquake:1-yr postseismic slip (color)
Updip segment off Peru:Not slipping. Fully relaxed?
Gagnon et al. (2005)
Very-low-frequency earthquakes possibly in Nankai accretionary prism
CORK fluid pressure transients associated with Nankai VLF
(Ito and Obara, 2006)
(Davis et al., 2006)
Fluid transients have also been observed at prism toe, Costa Rica, using flowmeters and also interpreted to indicate transient fault slip (Brown et al., 2005; Labonte et al., 2009).
Seismogenic zone
Questions:• What stops coseismic rupture at accretionary and erosional margins? • How does the updip segment move during the interseismic period? • How do stress and fluid in the wedge evolve throughout earthquake
cycles at accretionary and erosional margins?• What can we learn by observing subduction zones presently at
different stages of the earthquake cycle?
?
Bilek (2007)
smoothrough
very rough
Two aspects of the megathrust: 1) Fault zone material and its frictional behaviour2) Fault zone morphology and its scale variability
Frictional contact Uneven fault zone
Slip can break velocity-strengthening barrier, allowing large displacement in earthquakes. – localized shear
Large displacement requires modification of fault geometry, involving complex deformation of the fault-zone volume. – distributed cataclastic shear
Bilek (2007)
smoothrough
very rough
Two aspects of the megathrust: 1) Fault zone material and its frictional behaviour2) Fault zone morphology and its scale variability
Smoothly coupled fault;Rate-state friction;Giant earthquakes possible
Roughly coupled fault;Friction and complex deformation;Earthquakes and creep
Very roughly coupled fault;Complex fault zone deformation;Creep and small earthquakes