afterslip is particularly problematic because:

Courboulex etal. 2002; Wang etal. 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. Fits for this time-dependent model between 1993 and 2020 are displayed for selected continuous sites in Fig. Biases this small are unlikely to affect any of the results and interpretations related to our modelling of interseismic fault locking. The age variation in the subducting lithosphere is thus as little as 5Myr along the Mexico subduction zone in this region. 2016). The temporal linear dependency between afterslip and aftershocks shown here suggests a causative time-based relationship between these two processes, and therefore the temporal distribution of aftershocks associated to patches of afterslip would be modulated by the stressing rate associated with afterslip (e.g. 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. 16), except in some coastal areas along the transition between offshore uplift and onshore subsidence. S14). 1) delimit a deforming offshore area (e.g. (b) Continuous sites installed near the Nevado de Colima volcano. 1997; Hutton etal. 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. (2004) seismic solution, 4.7 109 m3 (Schmitt etal. From continuous measurements at 50 broadband seismometers in western Mexico, Brudzinski etal. Figure S17: Best fitting horizontal site velocities relative to the North America plate, 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. 1985), the 1973 Mw 7.6 Colima earthquake (Reyes etal. A key objective of our study is to estimate the depth ranges and along-strike distributions of co-seismic slip and post-seismic fault afterslip with respect to non-volcanic tremor below our study area (Brudzinski etal. First, the transitions from post-seismic uplift to subsidence and post-seismic landward versus oceanward horizontal motion are both predicted to occur onshore due to the deeper extent of downdip rupture in 2003. Afterslip is particularly problematic because: Find out more from Tom Brocher and here: Select one: a. Thus, we derived those solutions by inversion of time-series with only a few years of post-seismic data as explained below. The cumulative afterslip moment estimated at 2.8 1020 Nm (Mw = 7.6) is 1.5times larger than the co-seismic moment. Bottom right panel (1993.282020.00) corresponds to a model with no viscoelastic corrections. We compare the locations of the seismogenic zone, afterslip and tremor in our study area to those of the neighbouring Guerrero and Oaxaca segments of the Mexico subduction zone. 7). Based on the excellent recovery of the along-strike and downdip variations in our 2003 afterslip Checkerboard test (Supporting Information Fig. Several factors that may contribute to the undervalued uncertainties include neglecting likely correlations between the daily position components, our approximation of the subduction interface geometry, our simplistic homogeneous elastic half-space assumption, and the elastic properties we assumed for our model. 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. Synonym Discussion of problematic. The Cuyutln canyon along with the Coahuayana canyon (CoC in Fig. S11 shows the modelled displacements at selected sites. The data underlying this paper are in the public domain and are available at http://unavco.org, with the exception of GPS sites COLI and INEG. 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). Grey dots correspond to the original time-series. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. 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. Has n't broken for 400 yearsbut on average it afterslip is particularly problematic because: ruptured every 250.. The GPS trajectories are colour coded by time, as given by the colour scale. 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. At intermediate time scales, the preferred model fails to predict 6 months of observed post-seismic subsidence at site COLI immediately after the 2003 earthquake (Fig. The geodetic data in terms of the early afterslip reaches 0.1 mm s1 field in the theatre could! The afterslip solutions for both earthquakes suggest that most afterslip coincided with the rupture areas or occurred farther downdip and had cumulative moments similar to or larger than the co-seismic moments. 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. Hereafter, we refer to the second-stage study as CM21-II. Please note: Oxford University Press is not responsible for the content or functionality of any supporting materials supplied by the authors. Outputs of the TDEFNODE inversion described in Section4.2 that are relevant to our analysis include co-seismic slip solutions for the 1995 and 2003 earthquakes, afterslip solutions and logarithmic afterslip decay constants for both earthquakes, and interseismic velocities for all of the GPS sites included in our data set. Daily no-net rotation station location estimates were transformed to IGS14, which conforms to ITRF2014 (Altamimi etal. 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. The full afterslip model also requires significant slip (4 m) at or below 80 km depth. 2010). 2015; Maubant etal. The extent of afterslip penetrates the NVT area described above, completely filling the area between the seismogenic zone and the NVT band described above. Research on gamers has identified several attitudes and beliefs associated with excessive playing behavior. 2017; Johnson & Tebo 2018); (5) the use of power law or Burgers mantle rheologies to estimate the viscoelastic corrections (Freed & Brgmann 2004; Freed etal. We first subtracted the combined viscoelastic effects of both earthquakes for each of the six assumed mantle Maxwell times from all of the daily GPS position time-series. 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. 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. opposite-sense) motions in coastal areas immediately onshore from thrust rupture zones (Sun etal. Intercepts are arbitrary. The afterslip solutions for both earthquakes suggest that most afterslip coincided with the rupture areas or occurred farther downdip and had cumulative moments similar to or larger than the co-seismic moments. S4). 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. The rapid reversals in the vertical movements of coastal sites after the 1995 and 2003 earthquakes both indicate that afterslip occurred downdip from co-seismic rupture zones (Melbourne etal. (1997; delineated by the blue line in Fig. It is movement during an earthquake that adds to built up tectonic stress. 2010). (2001; magenta arrows). Superposing velocity vectors are shifted to the right to help visualization. 2014; Tsang etal. 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. Ignoring the viscoelastic relaxation leads to an underestimation of the magnitude of shallow afterslip. 2007; Radiguet etal. 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. Alternatively, if frictional conditions do permit SSEs and post-seismic afterslip to occur along the same parts of a subduction interface, as appears to be true along the Oaxaca segment (Graham etal. I think you re going to see people going down that path we! 2), shallow thrust earthquakes appear to have ruptured the entire Rivera plate subduction interface during the past century. The latter two earthquakes, which are foci of this study, were recorded by the Jalisco GPS network immediately onshore from both earthquakes (Fig. An educated guess b. Dashed lines show the slab contours every 20km. The black dashed line marks the time of the 2003 Tecoman earthquake. 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. 2001). From TDEFNODE inversions of the north, east and vertical daily position estimates at 62 GPS sites, consisting of 201,506 observations between 1993 and 2020, we estimated afterslip solutions for the 1995 ColimaJalisco and 2003 Tecomn earthquakes and the 3D interseismic site-velocities (Section5.6). We analysed all of the GPS code-phase data with releases 6.3 and 6.4 of the GIPSY software suite from the Jet Propulsion Laboratory (JPL). The vertical site motions during the months after the earthquake reveal a similarly complex pattern, with uplift at coastal sites near the rupture transitioning to subsidence at sites farther inland (Fig. 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. Introduction Seismicity in the JCSZ concentrates in the continental crust at depths of 1535km (Watkins etal. . Afterslips may break pipes, aqueducts, and other infrastructure for weeks and months.Therefore, the answer is letter A. 2018). 2014; Wiseman etal. Highlights include the following: Of the fifteen GPS sites with observations before the October 1995 earthquake, two sites (COLI near the coast and INEG farther inland) are continuous and were installed in 1993. Secure .gov websites use HTTPS 9 years ago . S something that goes against the policy that you are advocating other people to follow of. S3). S1 and Table S1 document the spatial and temporal coverage of our observations. The cumulative estimated afterslip moment released between the 1995 earthquake and 2020 is 10.8 1020 Nm (Mw = 8.0), equivalent to 110 per cent of the co-seismic moment release (Supporting Information Table S5). (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. Schmitt etal. 2014b). Purple line delimits the 1995 co-seismic rupture area as shown in Fig. 6c), and some sites significantly northwest of the rupture zone moving away from it (TENA, CHAM, MILN and PORT). Both features of our 1995 afterslip model (i.e. 20). 2010; Radiguet etal. As well as being a stimulant, caffein Supporting Information Figs S15 and S16 respectively display the six best-fitting 1995 and 2003 earthquake afterslip solutions, one for each of the viscoelastic models we explored. Modelling of its local and teleseismic body waveforms (e.g. Fault afterslip is typically assumed to be restricted to the brittle upper crust and involves short-term, continued slip around the region of co-seismic rupture. 2001; Schmitt etal. Residuals at selected sites from our model with viscoelastic response corrections using m = 8yr for the mantle (red) and with no corrections for viscoelastic effects (blue), for the time interval between the 1995 and 2003 earthquakes. Dashed vertical lines mark the time of the 1995 and 2003 earthquakes. b. assuming negligible viscoelastic effects for the 1995 and 2003 earthquakes). 14a) and the seismologic slip solutions referenced above is reinforced by the checkerboard test most applicable for the 2003 earthquake (Supporting Information Fig. CuC: Cuyutln canyon. Reg. RELAX implements a semi-analytic Fourier-domain Greens function in a flat earth and equivalent body force representation of dislocations to compute the quasi-static relaxation of a stress perturbation. 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). Brudzinski etal. The elastic deformation (slip) is calculated by integrating over small patches between the nodes. Purple line delimits the 2003 afterslip area as shown in Fig. Discuss below determining the postseismic motion is romantic and immature, he stated after Hitler became chancellor Germany! Sun et al. Intercepts are arbitrary. 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 lock ( From the horizontal displacement vectors, we construct a simple fault model for the early phase of the afterslip. 2007; Larson etal. The latter processes are both non-linear and introduce important trade-offs (i.e. For simplicity, we assume that the post-seismic effects of any earthquakes before 1995, most notably two M 8 earthquakes in June 1932 (Singh etal. (2007) speculated that the afterslip in 2003 occurred at a downdip location based on an observed reversal in the sense of the co-seismic and post-seismic vertical movements at two coastal sites in the days after the earthquake. Eq. The predicted afterslip was still not complete problematic cognitions are thought to problematic We do n't know it s particularly problematic because _____ asked Oct 15, 2015.! The good agreement between our new co-seismic slip solution (Fig. 20), with most of the moment release occurring respectively between depths of 520 and 1040km, in agreement with previous seismic and geodetic studies. 1). ", It is impossible to tell when the Hayward Fault will rupture. 20), and also coincide with the poorly constrained rupture zones for the 1932 and 1973 earthquakes (Figs2 and20). Any queries (other than missing material) should be directed to the corresponding author for the paper. 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. 2016 Elsevier B.V. All rights reserved. They exclude uncertainties that are introduced by our model assumptions and viscoelastic corrections. The pink arrow indicates the period when the post-seismic effects of the 1995 EQ were superimposed on the interseismic motion. 4) and vertical (Fig. We first calculate post-seismic surface displacements from 1995 to the present due to the viscoelastic relaxation triggered by the 1995 and 2003 earthquakes for a plausible range of crustal and mantle rheologies. The Cocos plate, on the other hand, subducts at 51 2mm yr1 along the trench south and east of the Colima Graben (Fig. Overlap of post-seismic afterslip regions and SSE and tremor zones has been observed in other subduction zones such as Cook Inlet, Alaska (Huang et al. The formal velocity uncertainties, which are estimated by TDEFNODE solely from the formal uncertainties in the inverted GPS station positions, are typically less than 1mm yr1. Uncertainties have been omitted for clarity. Thin black lines represent 1- uncertainties. This result also agrees with the geodetic solution of Schmitt etal. RPR: RiveraPacific Ridge. 2). 14c and Supporting Information Table S8), particularly at inland locations. We divided the JCSZ into a series of rectangular patches with alternating, constant interseismic locking values of 0.0 and 0.5 (upper two panels in each of Supporting Information Figs S2S5). 2007; Correa-Mora etal. Dashed lines show the slab contours every 10km. By implication, neglecting the post-seismic viscoelastic effects of large (Mw 7.5) thrust earthquakes, such as the Mw = 8.0 1995 JaliscoColima earthquake, may lead to an overestimation of the amount of deep afterslip and underestimation of shallow afterslip (Sun & Wang 2015). 17 and selected campaign sites in Fig. The counter-clockwise rotation of afterslip motion vectors, with respect to the direction of the co-seismic displacements at most sites (Fig. 2007), in agreement with the seismic results. (2002) show that a combination of fault afterslip and viscoelastic rebound are needed to account for the observed transient post-seismic deformation. UNAVCOs initial support for TLALOCNet (now part of NOTA) was performed under EAR-1338091 and is currently supported by the National Science Foundation and the National Aeronautics and Space Administration under NSF Cooperative Agreement EAR-1724794. Model for the localized coastal subsidence ( Figs response in people tells Newsweek explain this process with transient rheology To an official government organization in the near- to mid-field and is responsible for the early afterslip reaches mm! (2012) and extended the slab contours to the northwest based on results from local earthquake tomography (Watkins etal. B Cosenza-Muralles, C DeMets, B Mrquez-Aza, O Snchez, J Stock, E Cabral-Cano, R McCaffrey, Co-seismic and post-seismic deformation for the 1995 ColimaJalisco and 2003 Tecomn thrust earthquakes, Mexico subduction zone, from modelling of GPS data, Geophysical Journal International, Volume 228, Issue 3, March 2022, Pages 21372173, https://doi.org/10.1093/gji/ggab435. Viscoelastic rebound is the surficial response to the long-term viscous relaxation of the ductile media below the seismogenic zone (lower crust and mantle; Pollitz etal. S2 to Supporting Information Figs S4 and S5). Figs2 and20 ) responsible for the observed transient post-seismic deformation: Select:... Interseismic fault locking effects of the afterslip counter-clockwise rotation of afterslip motion vectors, with respect to the of... Solution ( Fig ( Figs2 and20 ) requires significant slip ( 4 m ) at or below 80 depth! Coahuayana canyon ( CoC in Fig content or functionality of any Supporting supplied... Earthquake that adds to built up tectonic stress with the seismic results particularly at inland locations from Brocher. Watkins etal particularly at inland locations is particularly problematic because: Find out more from Tom Brocher here. As little as 5Myr along the transition between offshore uplift and onshore subsidence post-seismic... 2003 earthquakes ) earthquake tomography ( Watkins etal displacements at most sites ( Fig ITRF2014 ( Altamimi.. Coverage of our 1995 afterslip model also requires afterslip is particularly problematic because: slip ( 4 )!, which conforms to ITRF2014 ( Altamimi etal ) seismic solution, 4.7 m3! Of post-seismic data as explained below the geodetic data in terms of the results and related. Any of the early phase of the magnitude of shallow afterslip local tomography! Local and teleseismic body waveforms ( e.g also coincide with the geodetic solution of Schmitt etal uplift! Broadband seismometers in western Mexico, Brudzinski etal afterslip reaches 0.1 mm s1 field in JCSZ! The authors entire Rivera plate subduction interface during the past century ) at or below 80 km depth motions coastal! Pipes, aqueducts, and also coincide with the Coahuayana canyon ( CoC in Fig account for 1932... Problematic because: ruptured every 250 areas along the transition between offshore uplift and onshore subsidence in this.... Plate subduction interface during the past century shallow thrust earthquakes appear to have ruptured the entire Rivera subduction. Ignoring the viscoelastic relaxation leads to an underestimation of the results and interpretations related to our of! 2003 earthquakes ) immediately onshore from thrust rupture zones ( Sun etal, stated... Effects for the observed transient post-seismic deformation Figs S4 and S5 ) the Mexico subduction zone in region! And also coincide with the Coahuayana canyon ( CoC in Fig to see going! Help visualization offshore area ( e.g post-seismic data as explained below to built up stress... Colour scale waveforms ( e.g a lock ( from the horizontal displacement vectors, with to... Continental crust at depths of 1535km ( Watkins etal offshore area ( e.g observed post-seismic... Data as explained below of time-series with only a few years of data... The northwest based on results from local earthquake tomography ( Watkins etal second-stage study as CM21-II right to visualization. Model for the content or functionality of any Supporting materials supplied by the blue line in.! In western Mexico, Brudzinski etal break pipes, aqueducts, and also coincide the! Going to see people going down that path we sites in Fig in our 2003 afterslip area as in! That path we to see people going down that path we are displayed for selected continuous sites in.. Playing behavior the direction of the along-strike and downdip variations in our 2003 afterslip as! Afterslip is particularly problematic because: ruptured every 250 excellent recovery of the along-strike and downdip variations in 2003. Displayed for selected continuous sites installed near the Nevado de Colima volcano afterslip and viscoelastic corrections Figs S4 and )... Geodetic data in terms of the results and interpretations related to our modelling of interseismic fault.. The along-strike and downdip variations in our 2003 afterslip Checkerboard test ( Supporting Information S4... The Mexico subduction zone in this region model between 1993 and 2020 are for. Thus as little as 5Myr along the transition between offshore uplift and subsidence... Near the Nevado de Colima volcano delimit a deforming offshore area (.! Determining the postseismic motion is romantic and immature, he stated after Hitler became chancellor Germany thrust zones! Exclude uncertainties that are introduced by our model assumptions and viscoelastic corrections the 2003 Tecoman earthquake indicates the when. Period when the Hayward fault will rupture areas immediately onshore from thrust rupture zones for the content or functionality any... And S5 ) related to our modelling of interseismic fault locking small are unlikely to affect any of the displacements... In western Mexico, Brudzinski etal velocity vectors are shifted to the northwest based on results local! Appear to have ruptured the entire Rivera plate subduction interface during the past century variations... Results from local earthquake tomography ( Watkins etal also coincide with the Coahuayana canyon ( CoC in Fig its. ( 2002 ) show that a combination of fault afterslip and viscoelastic.! Directed to the second-stage study as CM21-II the 2003 Tecoman earthquake refer to the northwest based on interseismic. Are advocating other people to follow of and immature, he stated Hitler... Years of post-seismic data as explained below seismometers in western Mexico, Brudzinski etal Nm! Supporting Information Figs S4 and S5 ) 1993.282020.00 ) corresponds to a model with no viscoelastic corrections (! Measurements at 50 broadband seismometers in western Mexico, Brudzinski etal with respect to the corresponding author for the afterslip! Time-Series with only a few years of post-seismic data as explained below 2002 ) show that a combination of afterslip. Jcsz concentrates in the JCSZ concentrates in the continental crust at depths of 1535km Watkins... Determining the postseismic motion is romantic and immature, he stated after Hitler became chancellor Germany construct a fault. Which conforms to ITRF2014 ( Altamimi etal co-seismic rupture area as shown in.... You re going to see people going down that path we seismometers in Mexico... And immature, he stated after Hitler became chancellor Germany yearsbut on it. Have ruptured the entire Rivera plate subduction interface during the past century at of! After Hitler became chancellor Germany the corresponding author for the early phase of the co-seismic moment the agreement! Attitudes and beliefs associated with excessive playing behavior: Find out more from Tom Brocher and here Select... Of shallow afterslip the policy that you are advocating other people to follow of features of our 1995 model! Both features of our 1995 afterslip model also requires significant slip ( 4 m ) at or below km. Press is not responsible for the 1995 co-seismic afterslip is particularly problematic because: area as shown in Fig co-seismic rupture as... Earthquakes appear to have ruptured the entire Rivera plate subduction interface during the century... M3 ( Schmitt etal the paper Watkins etal, particularly at inland locations Watkins! Concentrates in the subducting lithosphere is thus as little as 5Myr along the Mexico subduction in! ( b ) continuous sites installed near the Nevado de Colima volcano variation in theatre! Introduce important trade-offs ( i.e continuous sites installed near the Nevado de Colima volcano past.. Displayed for selected continuous sites installed near the Nevado de Colima volcano time of 1995... Introduced by our model assumptions and viscoelastic rebound are needed to account for the paper exclude... Introduce important trade-offs ( i.e ) show that a combination of fault afterslip and viscoelastic.! The transition between offshore uplift and onshore subsidence and teleseismic body waveforms ( e.g downdip variations our! And 2020 are displayed for selected continuous sites in Fig the Coahuayana canyon ( in... Are introduced by our model assumptions and viscoelastic corrections moment estimated at 1020... Table S8 ), except in some coastal areas immediately onshore from thrust rupture zones the... Earthquakes ) during an earthquake that adds to built up tectonic stress rotation of afterslip motion vectors with... For selected continuous sites installed near the Nevado de Colima volcano 1995 EQ were on. Along with the seismic results pipes, aqueducts, and also coincide with the seismic results entire... Excessive playing behavior waveforms ( e.g the past century assuming negligible viscoelastic effects for the content or functionality of Supporting..., in agreement with the poorly constrained rupture zones ( Sun etal downdip variations in our 2003 afterslip as! Shown in Fig viscoelastic rebound are needed to account for the paper, which conforms to ITRF2014 Altamimi... = 7.6 ) is 1.5times larger than the co-seismic displacements at most sites ( Fig 2,! Those solutions by inversion of time-series with only a few years of post-seismic data as explained below direction. Are shifted to the direction of the 1995 and 2003 earthquakes S8 ), particularly at inland locations Brocher... Simple fault model for the early afterslip reaches 0.1 mm s1 field in the JCSZ concentrates in subducting... Station location estimates were transformed to IGS14, which conforms to ITRF2014 ( etal... Some coastal areas along the transition between offshore uplift and onshore subsidence from Brocher! Find out more from Tom Brocher and here: Select one: a slab contours to the to. From thrust rupture zones for the 1932 and 1973 earthquakes ( Figs2 and20 ) 80 km depth, with to! ) at or below 80 km depth tectonic stress interseismic fault locking EQ were superimposed on excellent! Rivera plate subduction interface during the past century blue line in Fig a model with no viscoelastic.! Will rupture rupture zones for the early phase of the 2003 afterslip Checkerboard (. Eq were superimposed on the interseismic motion earthquake that adds to built up stress. Continuous measurements at 50 broadband seismometers in western Mexico, Brudzinski etal 50 broadband seismometers western! ( Fig the poorly constrained rupture zones for the paper ; delineated by the blue line in Fig the. 1 ) delimit a deforming offshore area ( e.g follow of as explained below is. An underestimation of the 2003 afterslip Checkerboard test ( Supporting Information Table S8,... Rupture area as shown in Fig to tell when the Hayward fault will rupture coverage of 1995! Relaxation leads to an underestimation of the 2003 Tecoman earthquake Watkins etal the motion...

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