Geodetic displacements and aftershocks following the 2001 M_w = 8.4 Peru earthquake: Implications for the mechanics of the earthquake cycle along subduction zones

Abstract

[1] We analyzed aftershocks and postseismic deformation recorded by the continuous GPS station AREQ following the M w = 8.4, 23 June 2001 Peru earthquake. This station moved by 50 cm trenchward, in a N235°E direction during the coseismic phase, and continued to move in the same direction for an additional 15 cm over the next 2 years. We compare observations with the prediction of a simple one-dimensional (1-D) system of springs, sliders, and dashpot loaded by a constant force, meant to simulate stress transfer during the seismic cycle. The model incorporates a seismogenic fault zone, obeying rate-weakening friction, a zone of deep afterslip, the brittle creep fault zone (BCFZ) obeying rate-strengthening friction, and a zone of viscous flow at depth, the ductile fault zone (DFZ). This simple model captures the main features of the temporal evolution of seismicity and deformation. Our results imply that crustal strain associated with stress accumulation during the interseismic period is probably not stationary over most of the interseismic period. The BCFZ appears to control the early postseismic response (afterslip and aftershocks), although an immediate increase, by a factor of about 1.77, of ductile shear rate is required, placing constraints on the effective viscosity of the DFZ. Following a large subduction earthquake, displacement of inland sites is trenchward in the early phase of the seismic cycle and reverse to landward after a time t i for which an analytical expression is given. This study adds support to the view that the decay rate of aftershocks may be controlled by reloading due to deep afterslip. Given the ratio of preseismic to postseismic viscous creep, we deduce that frictional stresses along the subduction interface account for probably 70% of the force transmitted along the plate interface.

Spatio-temporal Slip, and Stress Level on the Faults within the Western Foothills of Taiwan: Implications for Fault Frictional Properties

“…Assuming a hydrostatic pore pressure, a crustal density of 2.9, and a décollement depth of 10 km, it would imply a value of (a -b) of about 8 9 10 -3 . This value is in agreement with estimates derived from laboratory experiments which range from 5 9 10 -3 to 3.0 9 10 -2 (MARONE, 1998), or from postseismic observations, which fall in the range 10 -2 -10 -4 (HEARN et al, 2002;HSU et al, 2006;JOHNSON et al, 2006;MIYAZAKI et al, 2004;PERFETTINI and AVOUAC, 2004;PERFETTINI et al, 2005) …”

Earthquake and tsunami forecasts: Relation of slow slip events to subsequent earthquake rupture

“…SSEs in the same depth range have been reported in Alaska (48), Cascadia (49), and Japan (11,50), perhaps highlighting frictional conditions that also contribute to deep after-slip in subduction zones (51) and similarly help to define the extent of subsequent coseismic rupture (49).…”

Coseismic Slip and Afterslip of the GreatMw 9.15 Sumatra–Andaman Earthquake of 2004

“…It has been shown in some cases to coincide with the transition zone between the LFZ and the zone creeping at the long-term slip rate (Dragert et al, 1994;Mazzotti et al, 2003;Chlieh et al, 2004b). In most cases, even though some component of large-scale viscous relaxation might be present, deep afterslip seems to evolve as predicted by ratestrengthening frictional sliding (Montesi, 2004;Perfettini et al, 2005).…”