afterslip is particularly problematic because:
GPS station vertical trajectories for years 2003.082020.00. 2018) at the Instituto de Geofsica-Universidad Nacional Autnoma de Mxico (UNAM). 20). 2013); and 0.81.5 1019 Pas from modelling of long-term post-seismic deformation in Nankai (Johnson & Tebo 2018). Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few dozen GPS stations on land (e.g. Fig. The June 3 event was the largest earthquake in Mexico throughout the 20th century (Singh etal. Our processing methodology includes constraints on a priori tropospheric hydrostatic and wet delays from Vienna Mapping Function parameters (http://ggosatm.hg.tuwien.ac.at), elevation dependent and azimuthally dependent GPS and satellite antenna phase centre corrections from IGS08 ANTEX files (available via ftp from sideshow.jpl.nasa.gov) and FES2004 corrections for ocean tidal loading (holt.oso.chalmers.se). 2007), in agreement with the seismic estimates referenced above. 2012; Cavali etal. No previous afterslip solution for this earthquake has been estimated, although Schmitt etal. 4; also see Hutton etal. 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. 2013). Cumulative viscoelastic displacements for the 17-yr-long period 2003.06 to 2020.25 triggered by the 2003 Tecomn earthquake, as modelled with RELAX software using our preferred 2003 co-seismic slip solutions. 20). Westward-directed postseismic seafloor displacements may be due flow via low-temperature, plastic creep within the lower half of a Pacific lithosphere weakened by plate bending. The interval used for the inversion is shown in each panel. 15 sites refers to the use of the sites active during the earthquake exclusively. It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months. 2001; Schmitt etal. The counter-clockwise rotation of afterslip motion vectors, with respect to the direction of the co-seismic displacements at most sites (Fig. The combined viscoelastic effects of the 1995 and 2003 earthquakes for the 25-yr interval spanned by our study constitute a non-negligible fraction of the overall deformation within our study area during the past few decades. 2021). Dashed lines show the slab contours every 20km. (2) Early afterslip shows no evidence of a delayed nucleation or acceleration phase, where instead fault patches transition to immediate deceleration following rupture that is consistent with frictional relaxation under steady state conditions with dependence only on the sliding velocity. Our estimates of the size and location of the 1995 afterslip (orange area in Fig. Thought to maintain problematic gaming behaviors it s something that goes against the policy that you advocating! We measured the accumulation of postseismic surface slip on four, ~100-m-long alignment arrays for one year following the event. 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. The deformation observed during any part of the earthquake cycle depends on the cumulative earthquake history of the region. The sites with the largest differences are located along the coast close to the rupture area, where the predicted viscoelastic deformation is sensitive to small variations in the estimated co-seismic slip. 1997; Escobedo etal. 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! Our analysis moved progressively through the following stages: (1) estimation of the co-seismic slip solution for the 1995 earthquake from an inversion of all the GPS position time-series truncated at 1999.0 (Section5.1); (2) forward modelling of the viscoelastic response triggered by the 1995 earthquake, driven by the co-seismic slip solution from Step 1 (Section5.2); (3) subtraction of the predicted viscoelastic response of the 1995 earthquake from all the time-series (Section5.3); (4) estimation of the co-seismic slip solution for the 2003 earthquake from an inversion of all the GPS time-series corrected for the viscoelastic effects of the 1995 earthquake and truncated at 2005.5 (Section5.3); (5) forward modelling of the viscoelastic responses triggered by the 2003 earthquake, driven by the co-seismic slip solutions from Step 4 (Section5.4); (6) subtraction of the predicted viscoelastic responses of the 1995 and 2003 earthquakes from the original GPS time-series through early 2020 (Section5.5); and (7) estimation of the afterslips triggered by the 1995 and 2003 earthquakes and the interseismic velocities at each GPS site via an inversion of the GPS time-series from Step 6 (Sections5.5 and5.6). Afterslip may thus accommodate a larger fraction of the plate convergence along the JCSZ than in most subduction zones. Our modelling suggests that afterslip in 1995 and 2003 extended all the way downdip to the region of NVT on the Rivera/Cocos subduction interfaces (Fig. Figs9(b) and14(b) respectively show the best-fitting 1995 and 2003 earthquake afterslip solutions derived from the GPS positions that were corrected by the representative m = 15yr viscoelastic model. Any queries (other than missing material) should be directed to the corresponding author for the paper. Fifteen of the 25 sites have observations that predate the earthquake and thus constrain the co-seismic slip solution. 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. Figure S4: Checkerboard tests for the JaliscoColima subduction zone. Lowry etal. The 1973 rupture is from Reyes etal. \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. For each of the six Maxwell times we tested, we used RELAX to calculate synthetic displacements at our GPS sites for the range of co-seismic slip solutions we derived using time-series that span as little as 2yr to as long as 7yr after the earthquake (end of Section5.1). Modelled viscoelastic deformation for the 1995 ColimaJalisco earthquake at GPS sites active during the earthquake for mantle rheologies corresponding to Maxwell times of 2.5 (blue), 15 (red) and 40yr (green). (2002). The interseismic GPS site velocities, which are described and modelled by CM21-II, are summarized briefly in Section5.6. (2007) for the same interval from the early post-seismic motions at just two sites. The paradigm by which afterslip is thought of as the dominant postseismic mechanism immediately following earthquakes, with viscoelastic relaxation to follow in later years, is shown to no longer be valid. (2016). 14a). 2007; Selvans etal. The misfit, $$\begin{eqnarray*}
Because direct solvers consume too much memory for a large-scale problem, the CG method, a widely used iterative solver, was used. Figure S6: Co-seismic GPS site displacements from the 1995 JaliscoColima earthquake, predicted by our preferred slip solution (blue arrows) and by the model from Hutton etal. Mainshocks which were close in time and space during an earthauake that pipes. 2004; Yoshioka etal. AUTA, AYUT and GUFI) increased, whereas most inland sites subsided. 2004; Fig. It is movement during an earthquake that adds to built up tectonic stress. 1985), the 1973 Mw 7.6 Colima earthquake (Reyes etal. 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. Supp_Information_Cosenza-Muralles_etal_2021-I.pdf. Late-Night Drinking. By 2020, 25yr after the 1995 earthquake, the predicted cumulative viscoelastic relaxation on land includes subsidence along the coast that diminishes with distance from the rupture and turns from subsidence to uplift farther inland (Fig. Dashed lines show the slab contours every 20km. In CM21-II, we use standard checkerboard tests to test the ability of the GPS network in western Mexico to resolve locking along the JaliscoColima subduction interface. Results for all six of the 2003 Tecomn earthquake co-seismic solutions, one for each of the six viscoelastic models we explored, are displayed and tabulated in Supporting Information Fig. That you are advocating other people to follow afterslip reaches 0.1 mm s1,. 2001; Melbourne etal. 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. (2007) but differ at some locations in the vertical component (Supporting Information Fig. Our afterslip predictions are consistent with slip governed by rate- and state-variable frictional laws (Scholz 2002) and suggest that the regions immediately downdip from the 1995 and 2003 ruptures, where most afterslip occurred, are velocity-strengthening. 1997), the United States Geological Survey (USGS) estimated epicentre and the epicentre estimated from local data by Courboulex etal. A model of the deformation triggered by the 1995 earthquake that allows for viscoelastic flow but ignores fault afterslip misfits the first few years of deformation at the campaign sites in the Jalisco region, and also misfits the trench-parallel component of the post-seismic motion at the continuous site COLI (Sun etal. The smaller scatter after early 2003 was caused by a change in the GPS equipment. 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. 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. 2010). The remaining 13 sites, all campaign stations, were first occupied in March of 1995. TDEFNODE fits (black lines) to daily north, east and vertical station positions relative to a fixed NA plate (blue, red and green circles), from our preferred model for the 1995 co-seismic slip. 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. 20 of the main document. The yellow patch is the total estimated aftershock area of the 1932 June 3 and 18 earthquakes (Singh 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. Tremor east of the gap is instead mostly at depths of 5070km (Fig. 2016). The velocity ellipses show the 2-D, 1- uncertainties. 20 of the main document. To date, the absence (or infrequency) of moderate or large-magnitude SSEs appears to be the primary difference between how subduction is accommodated along the JCSZ versus the Guerrero and Oaxaca trench segments. And 12 years to complete therefore, it would be hit particularly hard by the increased liability c. prevents from. 2020). Introduction Locations of recent large thrust earthquakes (1973: purple, 1995: blue, 2003: green), afterslip (1995: orange, 2003: red) and non-volcanic tremor (grey dots) along the JaliscoColima subduction interface. What Is French Pudding Milk Tea,
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GPS station vertical trajectories for years 2003.082020.00. 2018) at the Instituto de Geofsica-Universidad Nacional Autnoma de Mxico (UNAM). 20). 2013); and 0.81.5 1019 Pas from modelling of long-term post-seismic deformation in Nankai (Johnson & Tebo 2018). Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few dozen GPS stations on land (e.g. Fig. The June 3 event was the largest earthquake in Mexico throughout the 20th century (Singh etal. Our processing methodology includes constraints on a priori tropospheric hydrostatic and wet delays from Vienna Mapping Function parameters (http://ggosatm.hg.tuwien.ac.at), elevation dependent and azimuthally dependent GPS and satellite antenna phase centre corrections from IGS08 ANTEX files (available via ftp from sideshow.jpl.nasa.gov) and FES2004 corrections for ocean tidal loading (holt.oso.chalmers.se). 2007), in agreement with the seismic estimates referenced above. 2012; Cavali etal. No previous afterslip solution for this earthquake has been estimated, although Schmitt etal. 4; also see Hutton etal. 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. 2013). Cumulative viscoelastic displacements for the 17-yr-long period 2003.06 to 2020.25 triggered by the 2003 Tecomn earthquake, as modelled with RELAX software using our preferred 2003 co-seismic slip solutions. 20). Westward-directed postseismic seafloor displacements may be due flow via low-temperature, plastic creep within the lower half of a Pacific lithosphere weakened by plate bending. The interval used for the inversion is shown in each panel. 15 sites refers to the use of the sites active during the earthquake exclusively. It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months. 2001; Schmitt etal. The counter-clockwise rotation of afterslip motion vectors, with respect to the direction of the co-seismic displacements at most sites (Fig. The combined viscoelastic effects of the 1995 and 2003 earthquakes for the 25-yr interval spanned by our study constitute a non-negligible fraction of the overall deformation within our study area during the past few decades. 2021). Dashed lines show the slab contours every 20km. (2) Early afterslip shows no evidence of a delayed nucleation or acceleration phase, where instead fault patches transition to immediate deceleration following rupture that is consistent with frictional relaxation under steady state conditions with dependence only on the sliding velocity. Our estimates of the size and location of the 1995 afterslip (orange area in Fig. Thought to maintain problematic gaming behaviors it s something that goes against the policy that you advocating! We measured the accumulation of postseismic surface slip on four, ~100-m-long alignment arrays for one year following the event. 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. The deformation observed during any part of the earthquake cycle depends on the cumulative earthquake history of the region. The sites with the largest differences are located along the coast close to the rupture area, where the predicted viscoelastic deformation is sensitive to small variations in the estimated co-seismic slip. 1997; Escobedo etal. 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! Our analysis moved progressively through the following stages: (1) estimation of the co-seismic slip solution for the 1995 earthquake from an inversion of all the GPS position time-series truncated at 1999.0 (Section5.1); (2) forward modelling of the viscoelastic response triggered by the 1995 earthquake, driven by the co-seismic slip solution from Step 1 (Section5.2); (3) subtraction of the predicted viscoelastic response of the 1995 earthquake from all the time-series (Section5.3); (4) estimation of the co-seismic slip solution for the 2003 earthquake from an inversion of all the GPS time-series corrected for the viscoelastic effects of the 1995 earthquake and truncated at 2005.5 (Section5.3); (5) forward modelling of the viscoelastic responses triggered by the 2003 earthquake, driven by the co-seismic slip solutions from Step 4 (Section5.4); (6) subtraction of the predicted viscoelastic responses of the 1995 and 2003 earthquakes from the original GPS time-series through early 2020 (Section5.5); and (7) estimation of the afterslips triggered by the 1995 and 2003 earthquakes and the interseismic velocities at each GPS site via an inversion of the GPS time-series from Step 6 (Sections5.5 and5.6). Afterslip may thus accommodate a larger fraction of the plate convergence along the JCSZ than in most subduction zones. Our modelling suggests that afterslip in 1995 and 2003 extended all the way downdip to the region of NVT on the Rivera/Cocos subduction interfaces (Fig. Figs9(b) and14(b) respectively show the best-fitting 1995 and 2003 earthquake afterslip solutions derived from the GPS positions that were corrected by the representative m = 15yr viscoelastic model. Any queries (other than missing material) should be directed to the corresponding author for the paper. Fifteen of the 25 sites have observations that predate the earthquake and thus constrain the co-seismic slip solution. 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. Figure S4: Checkerboard tests for the JaliscoColima subduction zone. Lowry etal. The 1973 rupture is from Reyes etal. \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. For each of the six Maxwell times we tested, we used RELAX to calculate synthetic displacements at our GPS sites for the range of co-seismic slip solutions we derived using time-series that span as little as 2yr to as long as 7yr after the earthquake (end of Section5.1). Modelled viscoelastic deformation for the 1995 ColimaJalisco earthquake at GPS sites active during the earthquake for mantle rheologies corresponding to Maxwell times of 2.5 (blue), 15 (red) and 40yr (green). (2002). The interseismic GPS site velocities, which are described and modelled by CM21-II, are summarized briefly in Section5.6. (2007) for the same interval from the early post-seismic motions at just two sites. The paradigm by which afterslip is thought of as the dominant postseismic mechanism immediately following earthquakes, with viscoelastic relaxation to follow in later years, is shown to no longer be valid. (2016). 14a). 2007; Selvans etal. The misfit, $$\begin{eqnarray*} Because direct solvers consume too much memory for a large-scale problem, the CG method, a widely used iterative solver, was used. Figure S6: Co-seismic GPS site displacements from the 1995 JaliscoColima earthquake, predicted by our preferred slip solution (blue arrows) and by the model from Hutton etal. Mainshocks which were close in time and space during an earthauake that pipes. 2004; Yoshioka etal. AUTA, AYUT and GUFI) increased, whereas most inland sites subsided. 2004; Fig. It is movement during an earthquake that adds to built up tectonic stress. 1985), the 1973 Mw 7.6 Colima earthquake (Reyes etal. 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. Supp_Information_Cosenza-Muralles_etal_2021-I.pdf. Late-Night Drinking. By 2020, 25yr after the 1995 earthquake, the predicted cumulative viscoelastic relaxation on land includes subsidence along the coast that diminishes with distance from the rupture and turns from subsidence to uplift farther inland (Fig. Dashed lines show the slab contours every 20km. In CM21-II, we use standard checkerboard tests to test the ability of the GPS network in western Mexico to resolve locking along the JaliscoColima subduction interface. Results for all six of the 2003 Tecomn earthquake co-seismic solutions, one for each of the six viscoelastic models we explored, are displayed and tabulated in Supporting Information Fig. That you are advocating other people to follow afterslip reaches 0.1 mm s1,. 2001; Melbourne etal. 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. (2007) but differ at some locations in the vertical component (Supporting Information Fig. Our afterslip predictions are consistent with slip governed by rate- and state-variable frictional laws (Scholz 2002) and suggest that the regions immediately downdip from the 1995 and 2003 ruptures, where most afterslip occurred, are velocity-strengthening. 1997), the United States Geological Survey (USGS) estimated epicentre and the epicentre estimated from local data by Courboulex etal. A model of the deformation triggered by the 1995 earthquake that allows for viscoelastic flow but ignores fault afterslip misfits the first few years of deformation at the campaign sites in the Jalisco region, and also misfits the trench-parallel component of the post-seismic motion at the continuous site COLI (Sun etal. The smaller scatter after early 2003 was caused by a change in the GPS equipment. 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. 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. 2010). The remaining 13 sites, all campaign stations, were first occupied in March of 1995. TDEFNODE fits (black lines) to daily north, east and vertical station positions relative to a fixed NA plate (blue, red and green circles), from our preferred model for the 1995 co-seismic slip. 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. 20 of the main document. The yellow patch is the total estimated aftershock area of the 1932 June 3 and 18 earthquakes (Singh 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. Tremor east of the gap is instead mostly at depths of 5070km (Fig. 2016). The velocity ellipses show the 2-D, 1- uncertainties. 20 of the main document. To date, the absence (or infrequency) of moderate or large-magnitude SSEs appears to be the primary difference between how subduction is accommodated along the JCSZ versus the Guerrero and Oaxaca trench segments. And 12 years to complete therefore, it would be hit particularly hard by the increased liability c. prevents from. 2020). Introduction Locations of recent large thrust earthquakes (1973: purple, 1995: blue, 2003: green), afterslip (1995: orange, 2003: red) and non-volcanic tremor (grey dots) along the JaliscoColima subduction interface.
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