Slow Slip Event On the Southern San Andreas Fault Triggered by the 2017 Mw8.2 Chiapas (Mexico) Earthquake

Tymofyeyeva, Ekaterina; Fialko, Yuri; Jiang, Junle; Xu, Xiaohua; Sandwell, David T.; Bilham, Roger; Rockwell, T. K.; Blanton, Chelsea M.; Burkett, Faith; Gontz, Allen; Moafipoor, Shahram

doi:10.1029/2018jb016765

Cited by 56 publications

(50 citation statements)

References 80 publications

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“…Dynamic triggering has been shown to influence the occurrence of earthquakes, aseismic slow earthquakes, tectonic tremors, landslides, and icequakes (Aiken et al., 2013; Gomberg et al., 1997; Gonzalez‐Huizar et al., 2012; H. P. Johnson et al., 2017; Obara, 2002; Peng et al., 2014; Tymofyeyeva et al., 2019; Wallace et al., 2017). Triggered shallow crustal earthquakes occur at a variety of fault systems, including subduction zones, continental plate boundaries, and geothermal fields (Brodsky et al., 2003; Fan & Shearer, 2016; Kaven, 2020; Nissen et al., 2016; Velasco et al., 2008; Yun et al., 2019).…”

Section: Introductionmentioning

confidence: 99%

Characteristics of Frequent Dynamic Triggering of Microearthquakes in Southern California

et al. 2021

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Earthquakes on separate faults can trigger and interact with each other (Freed, 2005; Hill & Prejean, 2015). Earthquakes triggered on receiver faults are often caused by the static and/or dynamic stress perturbations (Gomberg et al., 2001; Hill et al., 1993; King et al., 1994). The static triggering effects are most significant within a few fault lengths, while dynamic triggering can cause seismic events up to thousands of kilometers away (Harris, 1998; Velasco et al., 2008). Dynamic triggering due to passing seismic waves has been observed at various fault systems from near-field to far-field with stress perturbations ranging from ∼1 MPa to ∼0.1 kPa (e.g., Gomberg & Johnson, 2005; Kilb, 2003; van Der Elst & Brodsky, 2010). The large range of dynamic stress perturbations that can trigger earthquakes challenges our general understanding of earthquake failure initiation processes, particularly when triggering stresses are small. Understanding the role of

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Section: Introductionmentioning

confidence: 99%

Characteristics of Frequent Dynamic Triggering of Microearthquakes in Southern California

et al. 2021

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“…Stresses of <1 kPa due to deep SSEs and a large earthquake apparently triggered shallow SSEs along the plate interface in Costa Rica (Davis et al, 2015), and co‐seismic static stress changes of ~7 kPa from the M9.0 2011 Tohoku, Japan, earthquake may have initiated an SSE 900 km away along the shallow interface in the Nankai, Japan, subduction zone (Davis et al, 2013). Seismic wave‐generated dynamic stresses triggered SSEs at various depths from the M7.9 2001 Denali, Alaska, earthquake beneath Vancouver Island in the Cascadia subduction zone (40 kPa; Rubinstein et al, 2007); from the M8.8 2001 Maule, Chile, earthquake in the Guerrero segment of the Mexican SZ (~11 kPa; Zigone et al, 2012); and from the M8.2 2017 Chiapas, Mexico, earthquake along the shallow portion of the San Andreas Fault in California (~30 kPa; Tymofyeyeva et al, 2019). Shelly et al (2011) inferred that dynamic stresses from global and regional earthquakes as small as M5.4 triggered SSEs (noted as creep events) that then initiated bursts of tremor and small earthquake activity at 10–30 km depth along the Cholame section of the San Andreas Fault.…”

Section: Introductionmentioning

confidence: 99%

The Ocean's Impact on Slow Slip Events

Gomberg

Baxter

Smith

et al. 2020

Geophysical Research Letters

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We test the hypothesis that ocean seafloor pressures impart stresses that alter the initiation or termination of transient slow slip events (SSEs) on shallow submarine and near‐coastal faults, using simulated seafloor pressures and a new catalog of SSEs in the Hikurangi subduction zone. We show that seafloor pressures may be represented by an average time history over the ~100‐km dimensions of the study area. We account for SSE uncertainties and the multiplicity of processes that affect SSEs statistically by estimating the probabilities of rejecting the null hypothesis that SSE initiation or termination pressures are those to be expected by chance sampling of known (modeled) seafloor pressures, with low probabilities indicating some causal connection. No impact of ocean pressure changes on SSE initiation is detectable, but a correlation with their terminations is suggested. SSE slip that weakens the fault and makes it more sensitive to small stress changes may explain results.

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“…One contributing factor to this debate is that, in our chosen geometries, we use a SSAF Coachella strand that has a vertical dip from surface to depth. Recent geophysical observations (Fuis et al, 2017) and modeling efforts that incorporate both GPS and InSAR data sets in this area (Lindsey and Fialko, 2013;Fattaruso et al, 2014;Tymofyeyeva et al, 2019) indicate that the Coachella strand has a more complicated geometry than previously assumed by earlier modeling efforts such as the UCERF3 model and the SCEC CFM models. In particular, these investigations suggest that this strand may be dipping from 50°-70° to the northeast.…”

Section: Research Papermentioning

confidence: 99%

New geodetic constraints on southern San Andreas fault-slip rates, San Gorgonio Pass, California

et al. 2020

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Assessing fault-slip rates in diffuse plate boundary systems such as the San Andreas fault in southern California is critical both to characterize seismic hazards and to understand how different fault strands work together to accommodate plate boundary motion. In places such as San Gorgonio Pass, the geometric complexity of numerous fault strands interacting in a small area adds an extra obstacle to understanding the rupture potential and behavior of each individual fault. To better understand partitioning of fault-slip rates in this region, we build a new set of elastic fault-block models that test 16 different model fault geometries for the area. These models build on previous studies by incorporating updated campaign GPS measurements from the San Bernardino Mountains and Eastern Transverse Ranges into a newly calculated GPS velocity field that has been removed of long- and short-term postseismic displacements from 12 past large-magnitude earthquakes to estimate model fault-slip rates. Using this postseismic-reduced GPS velocity field produces a best-fitting model geometry that resolves the long-standing geologic-geodetic slip-rate discrepancy in the Eastern California shear zone when off-fault deformation is taken into account, yielding a summed slip rate of 7.2 ± 2.8 mm/yr. Our models indicate that two active strands of the San Andreas system in San Gorgonio Pass are needed to produce sufficiently low geodetic dextral slip rates to match geologic observations. Lastly, results suggest that postseismic deformation may have more of a role to play in affecting the loading of faults in southern California than previously thought.

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Slow Slip Event On the Southern San Andreas Fault Triggered by the 2017 M_w8.2 Chiapas (Mexico) Earthquake

Cited by 56 publications

References 80 publications

Characteristics of Frequent Dynamic Triggering of Microearthquakes in Southern California

Characteristics of Frequent Dynamic Triggering of Microearthquakes in Southern California

The Ocean's Impact on Slow Slip Events

New geodetic constraints on southern San Andreas fault-slip rates, San Gorgonio Pass, California

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