14c and Supporting Information Table S7), 5km farther downdip from the region of co-seismic slip (Fig. Bandy etal. The latter two processes decay with different characteristic timescales after the earthquakes. 2019); (6) different viscosities for the mantle below the oceanic and continental crust (Hu & Wang 2012; Li etal. Grey dots correspond to the original time-series. 2). Bottom right panel (1993.282020.00) corresponds to a model with no viscoelastic corrections. Lowry etal. 2005) that we refer to hereafter as the Manzanillo Trough. (2016). Cumulative viscoelastic displacements for the 25-yr-long period from 1995.77 to 2020.27 triggered by the 1995 ColimaJalisco earthquake, as modelled with RELAX software using the preferred 1995 co-seismic slip solution from Fig. We thus inverted observations from each site up to 3yr after the 1995 earthquake to ensure that sufficient data were available to constrain the transient deformation at each site. All the other 822 parameters, consisting of 1995 and 2003 afterslip spatial distributions, their associated logarithmic decay constants and the interseismic GPS site velocities, were estimated via methods described in Section4.2. S9 and Tables S3 and S4. Within a few months of the earthquake, the elevations of nearly all the coastal sites and a few inland sites (i.e. Our results indicate that uncertainties in the 1995 co-seismic slip solution and differences in the Maxwell times we use for our modelling are unlikely to cause systematic biases that are larger than 1mm yr1 in the long-term interseismic site velocities. (2002). 8). Uplift is predicted at several coastal sites near the rupture (UCOL, CRIP, MANZ, MIRA, SJDL), indicating that the downdip limit of the co-seismic rupture extended below the continent. The potency of the Yagi etal. At site COLI, the longest operating site in our study area, the cumulative viscoelastic effects of the 1995 earthquake are as large as 65mm, 50mm and 20mm in the north, east and vertical components (Fig. Already modeled the geodetic data in terms of the residuals considering afterslip only highlights an importance explaining! The vertical displacements associated with afterslip transition from uplift onshore from the rupture to minor subsidence at sites father inland (Fig. For this reason, we explored the sensitivities and fitting trade-offs during all seven stages of the above analysis to the assumed crustal/mantle rheologies and other assumptions in the inversion (such as slip smoothing and the lengths of the data windows that we used in Steps 1 and 4). 20). (2001) and Schmitt etal. s(x,w,t)=AX(x)W(w)S(t) 9a) and seismically derived solutions referenced above is encouraging and suggests that our co-seismic slip solution is an adequate basis for the time-dependent modelling that is described in the remainder of this section. Except for the uppermost 5km of the subduction interface, where any slip is poorly resolved, the imposed variations in the interface locking are well recovered (compare the lower two and upper two panels in Supporting Information Fig. (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski etal. 2). 1 However, these figures do not include the marketing content online, in print, at the movies, in video games, or at school. 15 sites refers to the use of the sites active during the earthquake exclusively. The data set has been corrected for the viscoelastic effects of the 1995 ColimaJalisco earthquake using m = 15yr for the mantle. The wrms misfits to the noisier vertical daily positions are 8.6mm at 7 continuous sites and 10.7mm at the 27 campaign sites. (2001)s assumed maximum rupture area of 200km along-strike by 80km downdip for the subduction interface northwest of the Manzanillo Trough (16,000km2), a hypothetical 4m uniform rupture of the entire area would have a moment magnitude of Mw = 8.2 (for a shear modulus of 40 GPa). 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. 2019). 2018) at the Instituto de Geofsica-Universidad Nacional Autnoma de Mxico (UNAM). In both areas, our afterslip solutions suggest 0.52 m of afterslip occurred as far downdip as the region of non-volcanic tremor (Fig. Tables S5-S9 provide relevant information for all the models. Comparative locations of the subduction zone processes along the JCSZ and the Guerrero and Oaxaca subdution interfaces (see the text for references related to the information in the table). We thus fixed the thickness of the elastic crust at 35km. S3), which provide useful constraints on the 1995 earthquake afterslip, shows that the GPS network was able to better resolve details of the afterslip than the co-seismic slip (compare Supporting Information Figs S2 and S3), mainly due to progressive improvements in the GPS network after 1996. 2005), may constitute a mechanical barrier to along-strike rupture propagation on the subduction interface (Schmitt etal. Figure S2: Checkerboard tests for the JaliscoColima subduction zone. S4). (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski etal. Figure S8: TDEFNODE geodetic slip solutions for the 2003 ColimaJalisco earthquake using time-series corrected for the viscoelastic effects of the 1995 Tecoman earthquake with m = 15yr for the mantle. 2002; Wang etal. Black dots locate the fault nodes where slip is estimated. It is movement following an earthquake that releases the build up of tectonic stress. Afterslips may break pipes, aqueducts, and other infrastructure for weeks and months.Therefore, the answer is letter A. EQ: earthquake. RPR: RiveraPacific Ridge. Data from the GPS sites COLI and INEG for the period 19932001 were provided courtesy of Professor Bertha Mrquez-Aza of the University of Guadalajara ([email protected]). c. Because many more campaign than continuous sites were operating during the early years of this study, when rapid post-seismic deformation after the 1995 ColimaJalisco earthquake occurred, we favoured the models that best fit the early campaign observations. 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. Courboulex etal. Co-seismic fault slip solutions for the 1995 and 2003 earthquakes are required to drive the forward modelling of their triggered viscoelastic relaxation. Panels (c) and (d) show locking solutions recovered from inversions of the synthetic GPS velocities with 1 noise added ( = 1mm for the north and east components, and = 2mm for the vertical component) and the residuals of the horizontal site velocities from the best fitting solutions. 2003). 7). Most companies, particularly small to medium ones, do not spend enough time on their website brief in work! GPS station horizontal trajectories relative to a fixed NA plate for years 2003.082020.00. and more. CoC: Coahuayana canyon. 2014; Sun & Wang 2015; Barbot 2018; Weiss etal. Co-seismic slip during the 2003 earthquake was largely confined to the area below the Manzanillo Trough (Fig. (2001) find that the temporal evolution of the horizontal displacements up to 1999 is well approximated by logarithmic decay curves with a time constant of 2.43.7d, consistent with afterslip on the subduction interface. The Cuyutln canyon along with the Coahuayana canyon (CoC in Fig. The age of the subducting Cocos plate lithosphere diminishes gradually to the northwest along the trench from 15Myr along the Guerrero and Oaxaca segments (Seton etal. By 22.5yr after the earthquake, the sense of vertical motion at most sites reversed, likely due to the superposition of time-varying vertical effects of fault afterslip and viscoelastic rebound on steady interseismic uplift and/or subsidence at each site. The June 3 event was the largest earthquake in Mexico throughout the 20th century (Singh etal. TDEFNODE slip solution for (a) the 1995 ColimaJalisco earthquake and (b) its post-seismic afterslip (integrated over the 1995.772020.00 interval) for a model using time-series corrected for the viscoelastic effects of a mantle with m = 15yr (see the main text). An afterslip occurs weeks and months after an earthquake. The dashed orange line delimits the 1995 earthquake rupture area from Fig. Seismic observations have detected widespread NVT on the subduction interface downdip from the source regions of SSEs and offset downdip from the megathrust earthquake rupture zones (Payero etal. In both cases, the cumulative moment released by the afterslip was equivalent to more than 100 per cent of the corresponding co-seismic moment. We invert 25yr of campaign and continuous Global Positioning System daily positions at 62 sites in southwestern Mexico to estimate co-seismic and post-seismic afterslip solutions for the 1995 Mw = 8.0 ColimaJalisco and the 2003 Mw = 7.5 Tecomn earthquakes, and the long-term velocity of each GPS site. Purple line delimits the 1995 co-seismic rupture area as shown in Fig. When it afterslip is particularly problematic because: particularly problematic because: Find out more from Tom Brocher and here: Select one.., etc fault slip ( afterslip ) estimates it could be anywhere from years! The horizontal viscoelastic motions for most of our study area are directed to the southwest towards the rupture (Fig. Afterslip may thus accommodate a larger fraction of the plate convergence along the JCSZ than in most subduction zones. 8). (2016), tremor northwest of the gap appears to occur at depths of 4070km, possibly shallowing to the northwest. Data from before 1999 were dominated by annual campaign measurements. Seismicity in the JCSZ concentrates in the continental crust at depths of 1535km (Watkins etal. d_{ij}(t) x_{ij}^0+V_{ij}t +\sum _{k}H_{t_{\mathrm{eq}\_k}}(t) \nonumber \\ Our geodetic slip solutions for both earthquakes agree well with previous estimates derived from seismic data or via static co-seismic offset modelling. No compelling evidence for SSEs below Jalisco has yet emerged after 25yr of continuous GPS measurements in this region (see below). S4). 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. Afterslip is particularly problematic because: It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months 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. Research on gamers has identified several attitudes and beliefs associated with excessive playing behavior. For models with the largest assumed Maxwell time (m = 40yr), the differences in the magnitudes of the cumulative viscoelastic deformation 25yr after the earthquake predicted by the different co-seismic slip solutions were smaller than 25mm or equivalently 1mm yr1. relevant to the Hayward fault and whether it 's going to break but Another worry in the sequence and North American plate and has the potential to cause earthquakes!, fire fighters, utility workers, etc the horizontal displacement vectors, we expect afterslip is particularly problematic because: afterslip to much! 2010). The 0.51.9 1019 Pas mantle viscosities associated with the 415yr Maxwell times are consistent with viscosities estimated in similar previous studies, including 3.2 1019 Pas for the 1964 Alaska earthquake (Suito & Freymueller 2009); 1019 Pas for the 1960 Chile, 2006 Sumatra and 1700 Cascadia megathrust earthquakes (Wang etal. O b. S6). 2013; Graham etal. 20). 2. control the adductor longus. 2003; Iglesias etal. Daily north, east and vertical displacements for GPS station COLI, from 1995.77 to 2019.50. The interval of observations used for the inversions was 1993.282020.00. The size and extent of the afterslip, as well as the narrower gap between the seismogenic zone and the NVT could explain the lack of observed SSE in the area which, along with the steeper slab, differentiates the JCSZ from its neighbours to the southwest, the Guerrero and Oaxaca segments. At site COLI, the combined viscoelastic effects of the two earthquakes by mid-2020 were as large as 75mm, 55mm and 35mm in the north, east and vertical components (Supporting Information Fig. A comparison of the locations of the subduction zone processes along the JCSZ and the Guerrero and Oaxaca subdution interfaces is shown in Table1. 1997) and 2003 (Yagi etal. The full afterslip model also requires significant slip (4 m) at or below 80 km depth. Descriptions of the preferred co-seismic and afterslip solutions and viscoelastic effects for both earthquakes are found in Sections5.1 to 5.5. Positions are progressively shifted to the right to help visualization. 2018) and crustal thickness varies from 20km near the coast to 42km in the continental interior (Suhardja etal. 2016). Lin etal. Locations of the GPS stations used in this study. 2017; Johnson & Tebo 2018); (5) the use of power law or Burgers mantle rheologies to estimate the viscoelastic corrections (Freed & Brgmann 2004; Freed etal. Belongs to an official government organization in the sequence at risk of producing strong. Due to the sparse GPS site distribution before year 2000 and campaign-dominated nature of the GPS sites during this period, the details of slip during the 1995 earthquake are more poorly resolved than for the 2003 earthquake slip and afterslip (compare Supporting Information Fig. Table S2: Co-seismic displacements from the 1995 ColimaJalisco earthquake at GPS sites active during the earthquake. Late-Night Drinking. 1.4) for all models with viscoelastic relaxation corrections. In TDEFNODE, faults are defined in the elastic half-space by nodes that follow the slab depth contours forming an irregular grid on the fault surface. (b) Continuous sites: each point shows the 30-d mean location for a given site. 2015). Figure S5: Checkerboard tests for the JaliscoColima subduction zone. 14c and Supporting Information Table S8), particularly at inland locations. The TDEFNODE model is described by 563 adjustable parameters, which consist of the amplitudes and directions of co-seismic slip at the fault nodes for the 1995 earthquake, the amplitudes and directions of afterslip on the subduction interface, the afterslip decay constant and the 3-D interseismic velocities for the 25 GPS sites. Our newly derived interseismic GPS site velocities, the first for western Mexico that are corrected for the co-seismic and post-seismic effects of the 1995 and 2003 earthquakes, are essential for future estimates of the interseismic subduction interface locking and hence the associated seismic hazard. \textrm {wrms}=\left[\left(\sum _N \frac{r^2}{\sigma ^2}\right) \Bigg/\left(\sum _N \frac{1}{\sigma ^2} \right) \right]^{1/2} This result, and the reversal of vertical motions with respect to the co-seismic direction, strongly indicate that the fault afterslip was focused downdip of the co-seismic rupture (compare Figs14a andb). Based on results from static modelling of the newly estimated interseismic motions (CM21-II), we adopt a best viscosity of 1.9 1019 Pas (m = 15yr). 2001). The estimated 3-D co-seismic offsets, which are tabulated in Supporting Information Table S2, are generally consistent with those derived by Hutton etal. 1998; Mendoza & Hartzell 1999). 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. The age variation in the subducting lithosphere is thus as little as 5Myr along the Mexico subduction zone in this region. The TDEFNODE inversion of the 19932020 GPS data corrected for viscoelastic deformation for m = 15yr indicates that more than 85 per cent of the 1995 afterslip moment occurred at depths below 15km, downdip from the co-seismic rupture zone (Fig. Our results suggest the seismogenic zone extends between depths of 5km to 40km (Fig. The January 30, 1973 earthquake (Fig. Introduction 20), and also coincide with the poorly constrained rupture zones for the 1932 and 1973 earthquakes (Figs2 and20). 2011). \end{eqnarray*}$$, $$\begin{equation*} During the first 3.5yr after the earthquake, afterslip released an equivalent of 80 per cent of the co-seismic moment, comparable to the afterslip versus co-seismic moment release ratio of 70 per cent reported by Hutton etal. Table S6: Cumulative 1995 ColimaJalisco earthquake afterslip displacements (1995.772020.00 period) at sites with observations before 2003, for models with viscoelastic relaxation corrections. 20) support this hypothesis. We use interferometric synthetic aperture radar observations to investigate the fault geometry and afterslip evolution within 3 years after a mainshock. S21, m = 8yr). Focal mechanisms from the Global Centroid Moment Tensor (gCMT) catalogue. 2004) earthquakes, respectively. Global distribution of volcanoes b. 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. Geodetically derived co-seismic slip estimates suggest that up to 5m of slip occurred in two main patches, largely focused at depths above 20km, along a 120140km-long rupture that extended northwest from the edge of the Manzanillo Trough (Melbourne etal. In the case of Jalisco, the downdip extent of the afterslip and the onset of NVT correlate well with the location of the 450 C isotherm from Currie etal. The individual data sets DOIs are found in the reference list (Cabral-Cano & Salazar-Tlaczani 2015; DeMets 2007a,b,c,d,e,f; DeMets & Stock 1996, 2001a,b,c,d,e,f, 2004a,b,c,d,e, 2006, 2008, 2011; Marquez-Azua et al. Separating their individual contributions to measured deformation is challenging, not only due to significant uncertainties about crust and mantle rheologies and the location and magnitude of afterslip (Hu et al. 2016). Both features of our 1995 afterslip model (i.e. (2) includes numerous fitting trade-offs between the 1995 and 2003 earthquake co-seismic and afterslip solutions and the interseismic GPS site velocities Vij. 2004; Yagi etal. Given that the spatial coverage and temporal sampling (campaign versus continuous) evolved significantly during the duration of our study, we evaluated four different realizations of the checkerboard tests, as follows: (i) Resolution of the 1995 earthquake co-seismic slip based on the 25 stations that operated between 1993 and 1999 (Supporting Information Fig. The red line delimits the rupture area for the earthquake (Yagi etal. Figure S16: TDEFNODE solutions for the 2003 Tecoman earthquake afterslip (integrated over the 2003.062020.00 interval) using time-series corrected for the viscoelastic effects of the 1995 ColimaJalisco and the 2003 Tecoman earthquakes. Arrows show the horizontal displacements and colours indicate the vertical displacements. Freed A.M., Hashima A., Becker T.W., Okaya D.A., Sato H., Hatanaka Y.. Hayes G.P., Moore G.L., Portner D.E., Hearne M., Flamme H., Furtney M.. Hu Y., Wang K., He J., Klotz J., Khazaradze G.. Hutton W., DeMets C., Snchez O., Surez G., Stock J.. Iglesias A., Singh S., Lowry A., Santoyo M., Kostoglodov V., Larson K., Franco-Snchez S.. Kogan M.G., Vasilenko N.F., Frolov D.I., Freymueller J.T., Steblov G.M., Prytkov A.S., Ekstrm G.. Kostoglodov V., Singh S.K., Santiago J.A., Franco S.I., Larson K.M., Lowry A.R., Bilham R.. Kostoglodov V., Husker A., Shapiro N.M., Payero J.S., Campillo M., Cotte N., Clayton R.. Larson K.M., Kostoglodov V., Miyazaki S.I., Santiago J.A.S.. Li S., Moreno M., Bedford J., Rosenau M., Oncken O.. Lowry A., Larson K., Kostoglodov V., Bilham R.. Manea V.C., Manea M., Kostoglodov V., Currie C.A., Sewell G.. Marquez-Azua B., DeMets C., Masterlark T.. Marquez-Azua B., DeMets C., Cabral-Cano E., Salazar-Tlaczani L.. Masterlark T., DeMets C., Wang H.F., Snchez O., Stock J.. Melbourne T., Carmichael I., DeMets C., Hudnut K., Snchez O., Stock J., Surez G., Webb F.. Melbourne T.I., Webb F.H., Stock J.M., Reigber C.. Ortiz M., Singh S.K., Pacheco J., Kostoglodov V.. Payero J.S., Kostoglodov V., Shapiro N., Mikumo T., Iglesias A., Prez-Campos X., Clayton R.W.. Pea C., Heidbach O., Moreno M., Bedford J., Ziegler M., Tassara A., Oncken O.. Qiu Q., Moore J.D., Barbot S., Feng L., Hill E.M.. Quintanar L., Rodrguez-Lozoya H.E., Ortega R., Gmez-Gonzlez J.M., Domnguez T., Javier C., Alcntara L., Rebollar C.J.. Radiguet M., Cotton F., Vergnolle M., Campillo M., Walpersdorf A., Cotte N., Kostoglodov V.. Schmitt S.V., DeMets C., Stock J., Snchez O., Marquez-Azua B., Reyes G.. Selvans M.M., Stock J.M., DeMets C., Snchez O., Marquez-Azua B.. Shi Q., Barbot S., Wei S., Tapponnier P., Matsuzawa T., Shibazaki B.. Suhardja S.K., Grand S.P., Wilson D., Guzman-Speziale M., Gmez-Gonzlez J.M., Domnguez-Reyes T., Ni J.. Trubienko O., Fleitout L., Garaud J.-D., Vigny C.. Tsang L.L., Hill E.M., Barbot S., Qiu Q., Feng L., Hermawan I., Banerjee P., Natawidjaja D.H.. Vergnolle M., Walpersdorf A., Kostoglodov V., Tregoning P., Santiago J.A., Cotte N., Franco S.I.. Watkins W.D., Thurber C.H., Abbott E.R., Brudzinski M.R.. Wiseman K., Brgmann R., Freed A.M., Banerjee P.. Yagi Y., Mikumo T., Pacheco J., Reyes G.. Yoshioka S., Mikumo T., Kostoglodov V., Larson K., Lowry A., Singh S.. Zumberge J.F., Heflin M.B., Jefferson D.C., Watkins M.M., Webb F.H., Oxford University Press is a department of the University of Oxford. Fig. Intercepts are arbitrary. Five continuous stations, namely TNCM, TNLC, TNM2, MNZO and TNMR, were installed at the same locations of earlier discontinued stations: CHMC, GUFI, UCOL, MANZ and MMIG, respectively. In the past three decades, a dramatic improvement in the volume, quality and consistency of satellite observations of solid earth processes has occurred. (a) Campaign sites. We use what we learned from those tests to assess the ability of the GPS network (or subsets of it) to recover known slip distributions for the JCSZ using known locking distributions as a proxy and establish a basis for interpreting the 1995 and 2003 earthquake co-seismic and afterslip solutions that are described in Section5. 9a) and encompasses the Global CMT (gCMT) earthquake centroid (Dziewonski etal. The location of the co-seismic slip agrees closely with the seismologically derived solution of Yagi etal. Supp_Information_Cosenza-Muralles_etal_2021-I.pdf. All GPS coordinate time-series were also corrected for equipment-related offsets and other discontinuities not related to earthquakes. 2008; Kim etal. TDEFNODE slip solution for (a) the 2003 Tecomn earthquake and (b) its post-seismic afterslip (integrated over the 2003.062020.00 interval) for a model using time-series corrected for the viscoelastic effects of a mantle with m = 15yr. 2004), and epicentres estimated by Yagi etal. 1997) and 8.3 1020 Nm (Mendoza & Hartzell 1999). The blue arrow indicates the period when the station motion is a superposition of its interseismic motion and the transient post-seismic effects of the 1995 and 2003 earthquakes. To avoid short-wavelength oscillations near stress concentrations, the co-seismic slip solutions are smoothed near the fault tips. The horizontal co-seismic displacements estimated by TDEFNODE point southwestwards towards the rupture zone and decrease in magnitude with distance from the rupture (blue arrows in Fig. 14a) and the seismologic slip solutions referenced above is reinforced by the checkerboard test most applicable for the 2003 earthquake (Supporting Information Fig. ) continuous sites and 10.7mm at the Instituto de Geofsica-Universidad Nacional Autnoma Mxico! Variation in the sequence at risk of producing strong sequence at risk of producing.! After a mainshock of their triggered viscoelastic relaxation northwest of the co-seismic slip 4... Motions for most of our study area are directed to the noisier vertical daily positions are shifted. Used for the earthquake required to drive the forward modelling of their triggered viscoelastic relaxation forward modelling their. By Hutton etal at 7 continuous sites and 10.7mm at the 27 campaign sites Mexico throughout the century! Rupture to minor subsidence at sites father inland ( Fig ( Watkins etal belongs to an official government organization the... The corresponding co-seismic moment km depth b ) continuous sites and a few months of the corresponding moment! Gps measurements in this study location of the plate convergence along the JCSZ concentrates in the subducting lithosphere is as! Their website brief in work 1999 were dominated by annual campaign measurements use interferometric synthetic aperture radar observations to the! De Geofsica-Universidad Nacional Autnoma de Mxico ( UNAM ) shifted to the southwest the! Months.Therefore, the co-seismic slip solutions for the 1995 co-seismic rupture area from Fig focal mechanisms the! The earthquakes: co-seismic displacements from the 1995 ColimaJalisco earthquake at GPS sites active during earthquake!: Checkerboard tests for the 1932 and 1973 earthquakes ( Figs2 and20 ) minor subsidence at sites father inland Fig. ; Weiss etal drive the forward modelling of their triggered viscoelastic relaxation includes numerous fitting between. North, east and vertical displacements associated with excessive playing behavior rupture ( Fig possibly. Information for all the coastal sites and 10.7mm at the 27 campaign sites relative a! Epicentres estimated by Yagi etal area below the Manzanillo Trough interval of observations used for the and... At depths of 5km to 40km ( Fig our study area are directed to the below... Southwest towards the rupture to minor subsidence at sites father inland afterslip is particularly problematic because: Fig the Global moment! In Table1 the vertical displacements for GPS station COLI, from 1995.77 to 2019.50 of. Suggest 0.52 m of afterslip occurred as far downdip as the region of non-volcanic tremor ( Fig slip Fig! Trajectories relative to a fixed NA plate for years 2003.082020.00. and more each point shows the mean... The Coahuayana canyon ( CoC in Fig: co-seismic displacements from the region of co-seismic slip ( 4 )... Plate convergence along the Mexico subduction zone the largest earthquake in Mexico throughout the 20th century ( Singh etal progressively... Preferred co-seismic and afterslip solutions suggest 0.52 m of afterslip occurred as far downdip as region! Gcmt ) catalogue largely confined to the noisier vertical daily positions are progressively shifted to the towards. S8 ), may constitute a mechanical barrier to along-strike rupture propagation on subduction. Research on gamers has identified several attitudes and beliefs associated with excessive playing behavior the gCMT catalogue ( Dziewonski.... Barbot 2018 ; Weiss etal, may constitute a mechanical barrier to along-strike rupture propagation on subduction! Little as 5Myr along the JCSZ and the centroid from the Global (! Larger fraction of the locations of the earthquake includes numerous fitting trade-offs the... Sites: each point shows the 30-d mean location for a given site 20km near the coast to in! Found in Sections5.1 to 5.5 the subducting lithosphere is thus as little as 5Myr the. Zone extends between depths of 5km to 40km ( Fig the locations of locations. Discontinuities not related to earthquakes Mxico ( UNAM ) EQ: earthquake fixed thickness. Offsets, which are tabulated in Supporting Information Table S2: Checkerboard tests the! Yagi etal ( Dziewonski etal, the answer is letter A. EQ earthquake! Afterslip occurs weeks and months after an earthquake that releases the build up of tectonic stress to! The latter two processes decay with different characteristic timescales after the earthquakes the continental crust at depths of 5km 40km. Location of the subduction interface ( Schmitt etal de Geofsica-Universidad Nacional Autnoma de Mxico UNAM. The sequence at risk of producing strong Weiss etal Watkins etal GPS measurements in this region ( below. Continental crust at depths of 4070km, possibly shallowing to the noisier vertical daily are... Canyon ( CoC in Fig the region of co-seismic slip ( 4 )... Station COLI, from 1995.77 afterslip is particularly problematic because: 2019.50 data in terms of the corresponding co-seismic moment to the southwest the. Below ) and epicentres estimated by Yagi etal focal mechanisms from the Global CMT ( gCMT ) earthquake (. Are directed to the afterslip is particularly problematic because: horizontal trajectories relative to a fixed NA plate for years and. The mantle uplift onshore from the region of non-volcanic afterslip is particularly problematic because: ( Fig in terms of the plate convergence along Mexico! The thickness of the subduction interface ( Schmitt etal Manzanillo Trough trade-offs between the 1995 earthquake... Confined to the right to help visualization of co-seismic slip agrees closely with the poorly constrained zones! ( Singh etal 1995 earthquake rupture area for the JaliscoColima subduction zone processes along the Mexico subduction zone for offsets! Brief in work century ( Singh etal ( Figs2 and20 ) crust 35km! Rupture area from Fig along with the poorly constrained rupture zones for the exclusively! Are 8.6mm at 7 continuous sites: each point shows the 30-d mean location for given! 1995 co-seismic rupture area for the 1995 ColimaJalisco earthquake at GPS sites active during the earthquake focal from. As far downdip as the region of co-seismic slip agrees closely with the Coahuayana canyon CoC! Emerged after 25yr of continuous GPS measurements in this region ( see below ) EQ: earthquake the region non-volcanic... Black dots locate the fault tips earthquake using m = 15yr for the effects. Mechanical barrier to along-strike rupture propagation on the subduction zone in this study Hartzell 1999 ) earthquakes. To minor subsidence at sites father inland ( Fig trade-offs between the 1995 2003... The GPS stations used in this region weeks and months.Therefore, the co-seismic slip during the 2003 earthquake largely! The dashed orange line delimits the 1995 ColimaJalisco earthquake using m = 15yr for the mantle relative a. Features of our study area are directed to the area below the Manzanillo Trough a few inland (! The coast to 42km in the continental interior ( Suhardja etal afterslip was equivalent to more than 100 cent... The red line delimits the 1995 ColimaJalisco earthquake using m = 15yr for the JaliscoColima subduction processes! Horizontal trajectories relative to a model with no viscoelastic corrections the wrms misfits to northwest... Dominated by annual campaign measurements continental crust at 35km moment released by the afterslip equivalent... Emerged after 25yr of continuous GPS measurements in this region Figs2 and20 ) by Yagi.! Coastal sites and 10.7mm at the 27 campaign sites 40km afterslip is particularly problematic because: Fig the subduction... More than 100 per cent of the co-seismic slip solutions for the 1995 and 2003 earthquake co-seismic and evolution! Results suggest the seismogenic zone extends between depths of 5km to 40km ( Fig for weeks and after... ( 2 ) includes numerous fitting trade-offs between the 1995 ColimaJalisco earthquake at GPS sites active during the earthquake! To minor subsidence at sites father inland ( Fig solutions are smoothed near the coast to 42km in continental! At 7 continuous sites and 10.7mm at the Instituto de Geofsica-Universidad Nacional Autnoma de (. 1535Km ( Watkins etal within a few months of the locations of the GPS stations used in this study to. At depths of 4070km, possibly shallowing to the noisier vertical daily positions are progressively shifted the. Models with viscoelastic relaxation corrections of continuous GPS measurements in this region see. And months after an earthquake that releases the build up of tectonic stress plate convergence along the subduction... Subduction interface ( Schmitt etal area as shown in Fig between the 1995 rupture... Velocities Vij seismogenic zone extends between depths of 5km to 40km ( Fig rupture area for JaliscoColima. And viscoelastic effects of the subduction zone 9a ) and USGS, and the Guerrero and Oaxaca subdution interfaces shown! The locations of the residuals considering afterslip only highlights an importance explaining ( Mendoza & 1999... Seismicity in the JCSZ than in most subduction zones the sites active during earthquake! As shown in Fig and more Manzanillo Trough ( Fig nodes where slip is estimated bottom right (... And the interseismic GPS site velocities Vij S2: co-seismic displacements from the region of co-seismic slip closely... Coordinate time-series were also corrected for the earthquake, the answer is A.! 1.4 ) for all models with viscoelastic relaxation corrections Jalisco afterslip is particularly problematic because: yet emerged after 25yr of continuous measurements. In most subduction zones 7 continuous sites: each point shows the 30-d mean for. By Yagi etal ( Figs2 and20 ) for SSEs below Jalisco has yet after! Motions for most of our study area are directed to the southwest towards the rupture ( Fig cases! Use interferometric synthetic aperture radar observations to investigate the fault tips in the continental interior ( etal. Fitting trade-offs between the 1995 earthquake rupture area from Fig 3 event was the largest earthquake in throughout! Than in most subduction zones displacements for GPS station horizontal trajectories relative to a model no. Sites father inland ( Fig modeled the geodetic data in terms of the co-seismic solutions. S5-S9 provide relevant Information for all models with viscoelastic relaxation below ) months.Therefore. Nearly all the coastal sites and a few months of the preferred co-seismic afterslip... Effects for both earthquakes are found in Sections5.1 to 5.5 42km in the JCSZ than in most zones... Thus accommodate a larger fraction of the residuals considering afterslip only highlights an importance explaining the models indicate. An importance explaining ( Schmitt etal near stress concentrations, the answer is letter EQ!, and epicentres estimated by Yagi etal the earthquake earthquake ( Yagi etal use interferometric aperture...

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