afterslip is particularly problematic because:

2020) and Nankai, Japan (Sherrill & Johnson 2021). The rapid post-seismic uplift rates decreased with time at the four sites nearest the rupture zone (i.e. 14d). 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. 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Seismicity in the JCSZ concentrates in the continental crust at depths of 1535km (Watkins etal. Figure S15: TDEFNODE slip solutions for the 1995 ColimaJalisco earthquake afterslip (integrated over the 1995.772020.00 interval) using time-series corrected for the viscoelastic effects of the 1995 ColimaJalisco and the 2003 Tecoman earthquakes. 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. The full afterslip model also requires significant slip (4 m) at or below 80 km depth. 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). Purple line delimits the 2003 afterslip area as shown in Fig. 2013); (4) incorporation of an elastic cold nose in the mantle wedge (Sun etal. 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. 2007; Selvans etal. 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. Arrows show the horizontal displacements and colours indicate the vertical displacements. 2015). Fig. Viscoelastic relaxation due to the 2003 earthquake (Fig. Best-fitting GPS site velocities from the time-dependent inversion of GPS position time-series that were corrected using a mantle Maxwell time of 15yr (Section5.6 and Supporting Information Table S10). 9c). We use interferometric synthetic aperture radar observations to investigate the fault geometry and afterslip evolution within 3 years after a mainshock. 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. Based on the slab geometry used in this study, which differs from that used by Brudzinski etal. (iii) Resolution of the 2003 earthquake co-seismic slip based on the 35 stations that operated between 1993 and 2005.5 and with data after 2003 (Supporting Information Fig. S8 are derived using 2.5yr or more of observations after the January 22, 2003 earthquake). Focal mechanisms for this earthquake indicate that it accommodated shallow underthrusting of the RI plate beneath the NA continental margin (Dziewonski etal. The sun and moon exert a gravitational tug on Earth that stretches and compresses crustal rocks. 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. Search for other works by this author on: Departamento de Estudios Socio Urbanos, Universidad de Guadalajara, Instituto de Geofsica, Universidad Nacional Autnoma de Mxico, Ciudad Universitaria, Caltech Seismological Laboratory, California Institute of Technology, Department of Geology, Portland State University, In TDEFNODE, the temporal and spatial distributions of slip on a fault during an event are described by, $$\begin{equation*} We found that the source regions for the 1995 and 2003 earthquakes ruptured distinctly different areas of the subduction interface (Fig. 1998; Mendoza & Hartzell 1999) indicate that the 150km-long rupture initiated at depths of 1520km near the Cuyutln submarine canyon (labelled CuC in 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. They also exclude uncertainties introduced by likely correlations between the daily GPS site position components. In both areas, our afterslip solutions suggest 0.52 m of afterslip occurred as far downdip as the region of non-volcanic tremor (Fig. 2002; Manea etal. and more. Superposing velocity vectors are shifted to the right to help visualization. AS: post-seismic afterslip; EQ: earthquake; IS: interseismic locking; VE: post-seismic viscoelastic rebound. Finite element model with transient mantle rheology to explain this process spatial pattern of evolution used any problematic language it About 10 % of the pandemic is particularly problematic because Paper and Assignments Academic. 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. The viscoelastic motions predicted for the 2003 Tecomn earthquake differ from the viscoelastic deformation triggered by the 1995 ColimaJalisco earthquake in two notable respects. 1). 1979), 1995 (Pacheco etal. It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months. Both exceed the typical <50 per cent afterslip-to-co-seismic moment release for subduction thrust earthquakes (Lin etal. Measurements at the nearby continuous sites COOB, MANZ and UCOL corroborate the short duration of the rapid post-seismic deformation (Fig. Our final solution from Step 7 above is corrected by viscoelastic deformation that is predicted by the 1995 and 2003 co-seismic slip solutions from Steps 1 and 4 above. (2016) suggest that the apparent lack of interseismic SSEs along the ColimaJalisco trench segment versus the abundance of large-magnitude SSEs below central and southern Mexico may be a consequence of the steeper dips of the subducting Rivera and northwesternmost Cocos plates, as well as the occurrence of significant earthquake afterslip along the narrow zone between the regions of shallow seismogenesis and downdip NVT in our study area. 2016). 9d). They exclude uncertainties that are introduced by our model assumptions and viscoelastic corrections. Our preferred time-dependent model for 1993.28 to 1999.0 is constrained by 3,371 observations consisting of the north, east and vertical daily position estimates at all 25 GPS sites (except for the vertical component at the far-field continuous station INEG, which is biased by rapid subsidence attributable to groundwater withdrawal). Prior to any modelling, we transformed each GPS position time-series from the ITRF14/IGS14 frame of reference to a frame of reference tied to the NA plate, the natural geological frame of reference for this study. Conversely, afterslip solutions that are associated with short Maxwell times and hence larger-magnitude viscoelastic deformation include some shallow afterslip and smaller-magnitude deep afterslip (also see Supporting Information Table S9). 2019, and figs 11 and 16). The Cocos plate, on the other hand, subducts at 51 2mm yr1 along the trench south and east of the Colima Graben (Fig. 20) support this hypothesis. 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. Dashed lines show the slab contours every 20km. S9) using their corresponding mantle Maxwell times (m = 2.5, 4, 8, 15, 25 and 40yr). Hu & Wang (2012) show that viscoelastic mantle relaxation and deep afterslip both cause trenchward motion of areas well inland from subduction-thrust rupture zones (Figs11 and16), such that ignoring the viscoelastic relaxation leads to overestimation of the deep afterslip (also see Sun etal. In the past three decades, a dramatic improvement in the volume, quality and consistency of satellite observations of solid earth processes has occurred. 2007; Radiguet etal. Another possible approach to improve the quality of fits is modelling multiple earthquake cycles while assuming plausible constitutive properties of nonlinear afterslip and viscoelastic rebound. 2007; Correa-Mora etal. 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). Black dots locate the fault nodes where slip is estimated. 2015; Maubant 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. , which differs from that used by Brudzinski etal afterslip occurred as far downdip as region. 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