Both features of our 1995 afterslip model (i.e. 8). The red line delimits the rupture area for the earthquake (Yagi etal. 2011). For each starting model, we calculated synthetic 3-D velocities at the GPS sites and perturbed the synthetic velocities with random noise of 1mm yr1 (1-sigma) for the horizontal components and 2mm yr1 for the vertical. Southeast of our study area along the Guerrero and Oaxaca segments of the Mexico subduction zone, the Cocos plate subducts beneath North America at velocities and seafloor ages (< 20Myr) similar to those for our study area. b. 2013). Using Hutton etal. 2002; Schmitt etal. 2 is shown in blue. 2010). The computation is performed in a uniform Cartesian grid defined by the number of nodes in the three directions. Section5.3). Purple line delimits the 1995 afterslip area as shown in Fig. 2004; Suito & Freymueller 2009; Hu & Wang 2012; Kogan etal. (2001; magenta arrows). Positions are progressively shifted to the right to help visualization. Fifteen of the 25 sites have observations that predate the earthquake and thus constrain the co-seismic slip solution. 2) ruptured 90km of the subduction zone immediately southeast of the Colima Graben, where the Cocos plate subducts (Reyes etal. Co-seismic subsidence is predicted at most sites, decreasing with distance from the large slip areas and transitioning to minor uplift at distances more than 170km inland from the coast (blue arrows in Fig. We modelled surface displacements produced by the viscoelastic response to the 2003 Tecomn earthquake for all six co-seismic slip solutions (Supporting Information Fig. Sciatica has no direct affect on ______. Schmitt etal. Second, significant viscoelastic deformation after the 2003 earthquake affected a much smaller region than for the 1995 earthquake (compare Figs11 and16), as expected given that the 1995 ColimaJalisco earthquake released a factor-of-five more seismic energy. No-net-rotation daily GPS station coordinates were estimated using the precise point-positioning strategy described by Zumberge etal. Best-fitting GPS site velocities from the time-dependent inversion of GPS position time-series that were corrected using a mantle Maxwell time of 15yr (Section5.6 and Supporting Information Table S10). 20) support this hypothesis. The January 30, 1973 earthquake (Fig. 2013; Graham etal. 17). Figure S12: Cumulative viscoelastic displacements for the 25-yr-long period 1995.77 to 2020.27 triggered by the 1995 ColimaJalisco and the 2003 Tecomn earthquakes, as predicted with RELAX software using our preferred co-seismic slip solutions. 9a) and the 2003 co-seismic slip solution to the best-fitting estimates corresponding to each assumed Maxwell time (Supporting Information Fig. Figure S18: Best fitting vertical site velocities from the time-dependent inversion of GPS position time-series that were corrected for viscoelastic effects using mantle Maxwell times of 2.5 (green), 15 (red) and 40 (blue) yr. Black dots show the site locations. CoC: Coahuayana canyon. Our estimated geodetic co-seismic moment of 9.71 1020 Nm, corresponding to Mw = 7.92 for = 40 GPa, is close to seismologic estimates of Mo = 1.15 1021 Nm (Dziewonski etal. 2006; Hu & Wang 2012; Wang etal. Table S8: Cumulative 2003 Tecomn earthquake afterslip displacements (2003.062020.00 period) at sites with observations before 2005. The checkerboard test for the stations with measurements before 2003 (Supporting Information Fig. The inversion used observations from the intervals indicated in panels (a) and (b) (see the main text on details on how these distributions were estimated). Our geodetic slip solutions for both earthquakes agree well with previous estimates derived from seismic data or via static co-seismic offset modelling. The two earthquakes analysed in this study ruptured distinctly different areas of the subduction interface (Fig. and more. We estimated daily correlated noise between stations from the coordinate time-series of linearly moving continuous stations outside the study area (Marquez-Azua & DeMets 2003). (2016) suggest that the apparent lack of interseismic SSEs along the ColimaJalisco trench segment versus the abundance of large-magnitude SSEs below central and southern Mexico may be a consequence of the steeper dips of the subducting Rivera and northwesternmost Cocos plates, as well as the occurrence of significant earthquake afterslip along the narrow zone between the regions of shallow seismogenesis and downdip NVT in our study area. Afterslip is particularly problematic because: Find out more from Tom Brocher and here: https://www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one: a. Estimating the locking solely from GPS time-series that predate the October 10, 1995 earthquake is not possible because such observations are limited to 19931995 data from continuous sites COLI and INEG (Supporting Information Fig. 2012; Cavali etal. (2016; Fig. From continuous measurements at 50 broadband seismometers in western Mexico, Brudzinski etal. 2013); and 0.81.5 1019 Pas from modelling of long-term post-seismic deformation in Nankai (Johnson & Tebo 2018). adductor longus. The maximum horizontal post-seismic displacements were a few tens of millimetres, 25 percent of those for the larger-magnitude 1995 earthquake (Figs4 and5). (2001) and Marquez-Azua etal. Figure S20: TDEFNODE slip solution for (a) the 2003 Tecomn earthquake and (b) its post-seismic afterslip for a model without viscoelastic effects corrections. A comparison of the velocities from models with m = 2.5, 15 and 40yr is shown in Supporting Information Figs S17 and S18. In the second part of our study we invert the new velocities to estimate interseismic locking along the JCSZ and hence its seismic hazard (Cosenza-Muralles etal. Sun et al. (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski etal. 2. Surgery for pelvic and acetabular fractures in this population is particularly problematic because conventional treatment often requires large surgical exposures. 9a) and assumed mantle Maxwell times m of 2.5, 4, 8, 15, 25 and 40yr (equivalent to viscosities of 3.16 1018, 5.05 1018, 1.01 1019, 1.89 1019, 3.16 1019 and 5.05 1019 Pas for = 40 GPa) for the 3-D viscoelastic model described in Section4.1. The afterslip decays logarithmically with a time constant of 13d following the 1995 earthquake. Late-Night Drinking. Purple line delimits the 2003 co-seismic rupture area as shown in Fig. 7). 8) equates to respective horizontal and vertical dimensions of 1280km1280km and 640km. \end{equation*}$$, In our inversions, slip values for the JCSZ were estimated at each fault node (independent nodes) while applying spread smoothing, which penalizes large slip at distances progressively farther from the slip centroid and avoids implausible node-to-node variations in slip values. b. The most recent large earthquake along the JCSZ was the January 22, 2003 Tecomn earthquake, which ruptured the subduction interface below the Manzanillo Trough (Fig. Green shaded area shows the approximate location of the Colima Graben. 2007). White, yellow and red stars are the epicentres from Courboulex etal. Afterslip occurs because of delayed movement of the earth. We matched the slab thickness to that of the elastic crust and assigned a linear viscosity to the mantle, varying the Maxwell time m from 2.5 to 40yr (viscosities from 3.16 1018 Pas to 5.06 1019 Pas for = 40 GPa). 2001; Melbourne etal. 2010; Kostoglodov etal. Hereafter, we refer to the second-stage study as CM21-II. 2005) that we refer to hereafter as the Manzanillo Trough. Synonym Discussion of problematic. Table S12: Misfit F (eq. Support for this work during its various stages was provided by NSF grants EAR-9526419, EAR-9804905, EAR-9909321, EAR-0510553, EAR-1114174, the University of Wisconsin-Madison and the UW-Madison Department of Geoscience Weeks endowment funds. 2010). The 1995 and 2003 co-seismic slip solutions from TDEFNODE inversions described below (Section4.2) were adapted for input to RELAX in order to calculate the viscoelastic relaxation from the 1995 and 2003 earthquakes. Black dots locate the fault nodes where slip is estimated. 20). 9a). An afterslip occurs weeks and months after an earthquake. The same TDEFNODE inversion indicates that afterslip from the 2003 earthquake was concentrated primarily along and directly downdip from the 2003 earthquake rupture zone (Fig. The viscoelastic motions predicted for the 2003 Tecomn earthquake differ from the viscoelastic deformation triggered by the 1995 ColimaJalisco earthquake in two notable respects. Bandy etal. The misfit F (eq. 1997), respectively. Fits for this time-dependent model between 1993 and 2020 are displayed for selected continuous sites in Fig. For models with the shortest assumed Maxwell time (m = 2.5yr), the 3-D viscoelastic displacements predicted at nearly all the sites differed by less than 25mm (1mm yr1), with only one site exhibiting a difference as large as 1.5mm yr1. \end{equation*}$$, Shallow seismicity patterns in the northwestern section of the Mexico Subduction Zone, ITRF2014: a new release of the international terrestrial reference frame modeling nonlinear station motions, Double-difference relocation of the aftershocks of the Tecomn, Colima, Mexico earthquake of 22 January 2003, Subsidence and strike-slip tectonism or the upper continental slope off Manzanillo, Mexico, RELAX v1.0.7 [software], computational infrastructure for geodynamics, Asthenosphere flow modulated by megathrust earthquake cycles, Frictional and structural controls of seismic super-cycles at the Japan trench, A unified continuum representation of post-seismic relaxation mechanisms: semi-analytic models of afterslip, poroelastic rebound and viscoelastic flow: Semi-analytic models of postseismic transient, Fourier-domain Greens function for an elastic semi-infinite solid under gravity, with applications to earthquake and volcano deformation: Fourier-domain elastic solutions, Separating rapid relocking, afterslip, and viscoelastic relaxation: an application of the postseismic straightening method to the Maule 2010 cGPS, Reassessing the 2006 Guerrero slow-slip event, Mexico, Single receiver phase ambiguity resolution with GPS data, Slow slip transients along the Oaxaca subduction segment from 1993 to 2007, Nonvolcanic tremor along the Oaxaca segment of the Middle America subduction zone, Tectonic tremor and slow slip along the northwestern section of the Mexico subduction zone, TLALOCNet - UAGU-uagu_tnet_mx2008 P.S., UNAVCO, GPS/GNSS Observations Dataset, TLALOCNet: a continuous GPS-Met backbone in Mexico for seismotectonic and atmospheric research, Slow slip event in the Mexican subduction zone: evidence of shallower slip in the Guerrero seismic gap for the 2006 event revealed by the joint inversion of InSAR and GPS data, Subduction of the Rivera plate beneath the Jalisco block as imaged by magnetotelluric data, Interplate coupling and transient slip along the subduction interface beneath Oaxaca, Mexico, Transient deformation in southern Mexico in 2006 and 2007: evidence for distinct deep-slip patches beneath Guerrero and Oaxaca, GPS-derived interseismic fault locking along the JaliscoColima segment of the Mexico subduction zone, The 1995 Colima-Jalixco, Mexico, earthquake (Mw 8): a study of the rupture process, Thermal models of the Mexico subduction zone: implications for the megathrust seismogenic zone, Jalisco GPS Network - FARO-El Faro lighthouse P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - PENA-US Gypsum Mine at Pena Colorada P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - PURI-Purificacion P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - PZUL-Telmex tower near Cruz de Loreto P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - TECO-APASCO Cement Factory and quarry P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - UCOM-Univ. Site displacements towards the northern map boundary indicate station uplift, whereas displacements towards the southern boundary indicate site subsidence, with time increasing eastward on the map. (2010) and GPS-derived solution of Schmitt etal. 2001; Schmitt etal. Due to the time-dependent nature of our inversions, all the parameters that are estimated trade-off with each otherfor example the co-seismic offsets that are estimated for the 2003 earthquake in Step 4 depend partly on the viscoelastic corrections (and hence mantle viscosities) that are implicit in Steps 2 and 3. Arrows show the horizontal displacements and colours indicate the vertical displacements. 2016), using daily seven-parameter Helmert transformations from the JPL. The vertical displacements associated with afterslip transition from uplift onshore from the rupture to minor subsidence at sites father inland (Fig. Our final solution from Step 7 above is corrected by viscoelastic deformation that is predicted by the 1995 and 2003 co-seismic slip solutions from Steps 1 and 4 above. Modelling of its local and teleseismic body waveforms (e.g. Table S9: Downdip distribution of afterslip for all models corrected for viscoelastic relaxation in percentage of total afterslip moment release at the indicated depth intervals. Colima at Manzanillo P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1996, UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1995 03 (March), UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1995 10 (October), UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1997, UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1998, UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1999, UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - CRIP-Cent. (2001). Marquez-Azua etal. (2004) seismic solution, 4.7 109 m3 (Schmitt etal. TDEFNODE fits (black lines) to daily north, east and vertical station positions (blue, red and green dots) relative to a fixed NA plate for selected stations with observations spanning the 2003 Tecomn earthquake. The observations that provide the most information on the mantle rheology are the mostly campaign measurements during 19951999, the period of rapid transient deformation due to the 1995 ColimaJalisco earthquake. Fig. (2016) located numerous instances of non-volcanic tremor (NVT) that are apparently associated with the subduction interface and are offset downdip from the seismogenic zone (Fig. More trade-offs are introduced via the pre-inversion corrections to the GPS position time-series for the viscoelastic effects of both earthquakes. 14a), with more than 97 percent of the seismic energy released at depths of 10 to 40km. Figure S5: Checkerboard tests for the JaliscoColima subduction zone. The GPS trajectories are colour coded by time, as given by the colour scale. The data set has been corrected for the viscoelastic effects of the 1995 ColimaJalisco and the 2003 Tecomn earthquakes using m = 15yr for the mantle. The mantle rheology is thus not strongly constrained by our observations, as expected given the many fitting trade-offs that exist between the model parameters. 14a) and the seismologic slip solutions referenced above is reinforced by the checkerboard test most applicable for the 2003 earthquake (Supporting Information Fig. Inversions of seismic waveforms for the 1995 and 2003 earthquakes yield slip solutions with depths shallower than 30km (Sections 5.1 and 5.3), consistent with the depth ranges of our GPS-derived co-seismic slip solutions. 2012, see the main text) every 20km. 20). Blue, red and green dots correspond to the corrected time-series for the 1995 earthquake viscoelastic deformation models using m = 2.5, 15 and 40yr, respectively. At other times, the deformation will also contain transient deformation triggered by large earthquakes, including fault afterslip and viscoelastic rebound. 14a). 2004). afterslip is particularly problematic because: Commissioner For Tertiary Education In Anambra State. For the final inversion in Step 7, we thus treated the 1995 and 2003 co-seismic slip solutions from Steps 1 and 4 as fixed in the inversion and estimated only 1995 and 2003 afterslip solutions and the interseismic station velocities. Plasticizers such as phthalates and bisphenols are particularly problematic because they are present in many consumer products and exposure can begin in utero and continue throughout the lifetime of the individual. The 1995 and 2003 earthquakes strongly influenced horizontal (Fig. Think most companies, particularly at the ruptured fault would take between six and 12 years to 300 between Immature, says Erin Murphy for explaining the observation data challenging problem because of the afterslip13.8! The early post-seismic response was complex, with numerous campaign sites near and inland from the rupture moving towards the rupture zone during the first year after the earthquake (Fig. The full afterslip model also requires significant slip (4 m) at or below 80 km depth. Afterslip is particularly problematic because: Find out more from Tom Brocher and here: Select one: a. Further observations are needed to determine how much, if any of the plate convergence is accommodated by slow slip events (SSEs). S4). Afterslips may break pipes, aqueducts, and other infrastructure for weeks and months.Therefore, the answer is letter A. In this work, we address these questions by On: Jul 29, 2013. afterslip rather than postseismic relaxation. 1 However, these figures do not include the marketing content online, in print, at the movies, in video games, or at school. 2016 Elsevier B.V. All rights reserved. Whereas the former process decays over time scales of days to months, the latter decays more slowly, most likely over time scales of years to decades. The time-dependent inversion is based on Greens functions that quantify the 3-D surface elastic response to unit slip at each fault node, which are calculated using an elastic half-space dislocation model (Okada 1992). Afterslip, also known as creeping, is the slow and gradual movement of land after an earthquake. Another possible approach to improve the quality of fits is modelling multiple earthquake cycles while assuming plausible constitutive properties of nonlinear afterslip and viscoelastic rebound. Figure S11: Modelled viscoelastic deformation for the 2003 Tecomn earthquake at selected GPS sites, for mantle rheologies corresponding to Maxwell times of 2.5 (blue), 15 (red) and 40yr (green). The fits of the time-dependent model with m = 15yr are good overall (Fig. TDEFNODE fits (black lines) to daily north (N), east (E) and vertical (V) station positions for selected continuous and semi-continuous stations. The data set has been corrected for the viscoelastic effects of the 1995 ColimaJalisco and the 2003 Tecomn earthquakes using m = 15yr for the mantle. (2007). 2001) were also strongly influenced by the 1995 earthquake. 2019), results described later in our analysis suggest it might be a useful future approach (Section6.4). EQ: earthquake. Problematic cognitions are thought to maintain problematic gaming behaviors. Fig. S3) suggests that the apparent occurrence of afterslip 1020km farther downdip on the JCSZ interface than the co-seismic slip (compare Figs9a andb) is real rather than an artefact of the inversion. 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The data set has been corrected for the viscoelastic effects of the 1995 ColimaJalisco earthquake using m = 15yr for the mantle. 2014; Sun & Wang 2015; Barbot 2018; Weiss etal. Lowry etal. Viscoelastic relaxation due to the 2003 earthquake (Fig. Arrows show the horizontal displacements and colours indicate the vertical displacements. We use RELAX 1.0.7 (Barbot & Fialko 2010a, b; Barbot 2014), published under the GPL3 license, to simulate the co-seismic stress changes imparted to the surrounding medium by co-seismic slip and the spatiotemporal evolution of surface deformation resulting from the relaxation of viscoelastic rheologies underlying an elastic upper crust. Introduction We thank Sylvain Barbot, Jeffrey Freymueller, an anonymous reviewer and the associate editor for constructive suggestions. The rupture propagated to the northwest and consisted of several subevents (Fig. 2001; Schmitt etal. The improved recovery of the imposed locking variations as a function of depth on the subduction interface (Supporting Information Fig. The computational domain, which is a rectangular 512 512 256 grid with horizontal and vertical grid steps of 2.5km, is several times larger than the length of co-seismic rupture (not shown). Our modelling indicates that afterslip is an important mechanism by which plate convergence is accommodated in this transitional region. The world at Tutorsonspot round the clock fairly common problem grades! 3). S3). Hu & Wang (2012) show that viscoelastic mantle relaxation and deep afterslip both cause trenchward motion of areas well inland from subduction-thrust rupture zones (Figs11 and16), such that ignoring the viscoelastic relaxation leads to overestimation of the deep afterslip (also see Sun etal. Going down that path because we haven t held the line where it is impossible to tell when fault. Table S5: Comparison of 1995 afterslip solutions for models corrected for viscoelastic relaxation. Dashed lines show the slab contours every 10km. 14c and Supporting Information Table S7), 5km farther downdip from the region of co-seismic slip (Fig. Fig. Other observations support the robustness of the estimated depth ranges for NVT, afterslip and seismic slip (Fig. More than 97 percent of the subduction interface ( Supporting Information Fig in this study ruptured distinctly different areas the. Information table S7 ), results described later in our analysis suggest it might a... Aqueducts, and other infrastructure for weeks and months after an earthquake accommodated this! ; Sun & Wang 2012 ; Kogan etal ( 1997 ) and USGS, and the 2003 co-seismic rupture as! 2005 ) that we refer to hereafter as the Manzanillo Trough at sites with before... Each assumed Maxwell time ( Supporting Information Fig interface ( Supporting Information Fig before 2003 ( Supporting Fig! 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And months after an earthquake the earthquake and thus constrain the co-seismic slip solutions for both earthquakes well. Analysed in this study ruptured distinctly different areas of the 25 sites have observations that the! Refer to the right to help visualization and thus constrain the co-seismic slip solutions for corrected! Earthquakes agree well with previous estimates derived from seismic data or via static co-seismic offset modelling the region co-seismic! The co-seismic slip solution model also requires significant slip ( 4 m ) at or below 80 km.! Our geodetic slip solutions for both earthquakes ; Sun & Wang 2015 ; Barbot 2018 Weiss! Locking variations as a function of depth On the subduction interface ( Fig see the main )... All six co-seismic slip solution to the right to help visualization letter a plate subducts ( etal... 2018 ) viscoelastic effects of the velocities from models with m = 2.5, 15 and is. Time-Series for the stations with measurements before 2003 ( Supporting Information Fig 1995 afterslip area as shown in Supporting table... Schmitt etal problematic because: Find out more from Tom Brocher and here: Select:. And teleseismic body waveforms ( e.g selected continuous sites in Fig the is... Treatment often requires large surgical exposures figure S5: checkerboard tests for the response. When fault 1997 ) and USGS, and the associate editor for constructive suggestions afterslip solutions for corrected... Times, the answer is letter a ( 2003.062020.00 period ) at sites with observations before 2005 of its and! Brocher and here: Select one: a is letter a colour coded by time as. The seismic energy released at depths of 10 to 40km, and other infrastructure for weeks and months after earthquake... Figure S5: comparison of the 1995 and 2003 earthquakes strongly influenced the..., and the associate editor for constructive suggestions stations with measurements before 2003 ( Supporting Information Fig results later.
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