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2019), results described later in our analysis suggest it might be a useful future approach (Section6.4). The seismicity suggests distributed shear across a diffuse RiveraCocos plate boundary (DeMets & Wilson 1997). We measured the accumulation of postseismic surface slip on four, ~100-m-long alignment arrays for one year following the event. This suggests that afterslip and SSEs, which originate from different stress conditions, may share similar physical conditions and that the onset of afterslip can reduce the amount of accumulated stress available to drive SSEs (Huang et al. 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. Figure S12: Cumulative viscoelastic displacements for the 25-yr-long period 1995.77 to 2020.27 triggered by the 1995 ColimaJalisco and the 2003 Tecomn earthquakes, as predicted with RELAX software using our preferred co-seismic slip solutions. The along-strike variations are particularly well recovered, which indicates that the slip during the 2003 earthquake was strongly concentrated offshore from the southern Colima Graben (Fig. `` [ the findings are ] relevant to others that have very characteristics. (iv) Resolution of the 2003 earthquake afterslip based on the 59 stations that operated between 1993 and 2020 and with data after 2003. For example, during the years immediately after the 1995 Mw = 8.0 ColimaJalisco earthquake, nearly all the sites in our study area moved southwestward towards the 1995 earthquake rupture zone at rates that decreased with time (Fig. The 1995 and 2003 afterslip estimates that are derived assuming mantle Maxwell times other than 15yr generally concur with the estimate described above (i.e. 2004; Suito & Freymueller 2009; Hu & Wang 2012; Kogan etal. Grey dots correspond to the original time-series. Tectonic setting. Locations of the GPS stations used in this study. 2). 2013; Sun etal. The Cocos plate, on the other hand, subducts at 51 2mm yr1 along the trench south and east of the Colima Graben (Fig. But closer to the surface, the earth had the. The JaliscoColima subduction zone (hereafter abbreviated JCSZ), at the northern end of the Mexico subduction zone (MSZ) and offshore from western Mexico, accommodates northeastward subduction of the Rivera (RI) and Cocos (CO) plates beneath the western edge of the North America (NA) plate (Fig. The two earthquakes analysed in this study ruptured distinctly different areas of the subduction interface (Fig. Fig. And 12 years to complete therefore, it would be hit particularly hard by the increased liability c. prevents from. For comparison, the mean value of the average slip and the area from our models of the 2003 earthquake rupture were 0.8m and 5,800km2, respectively. 2). 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. 2007; Radiguet etal. (2004) seismic solution, 4.7 109 m3 (Schmitt etal. The post-seismic transient deformation since 1995 has been tracked by measurements at campaign and continuous GPS stations in western Mexico. 3) varied by only 10 per cent for the wide range of mantle Maxwell times we tested (Supporting Information Table S12), including an inversion of the GPS position time-series without any viscoelastic corrections (Supporting Information Section S1, Tables S3, S5, S7, S9 and S11, and Figs S19 and S20). It furthers the University's objective of excellence in research, scholarship, and education by publishing worldwide, This PDF is available to Subscribers Only. The maximum horizontal post-seismic displacements were a few tens of millimetres, 25 percent of those for the larger-magnitude 1995 earthquake (Figs4 and5). 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 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. The co-seismic slip in our model is imposed via slip on a collection of patches that discretize the fault geometry. In the along-strike direction, the afterslip occurred mainly within the along-strike boundaries of the co-seismic rupture (Fig. It can develop in both men and women, particularly in people who smoke, drink excessive amounts of alcohol, take steroid medication, or have a family history of hip fractures. 2) ruptured 90km of the subduction zone immediately southeast of the Colima Graben, where the Cocos plate subducts (Reyes etal. (2007) but differ at some locations in the vertical component (Supporting Information Fig. The crisscrossing of the nerve fibers from the various . 15 sites refers to the use of the sites active during the earthquake exclusively. Synonym Discussion of problematic. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. Purple line delimits the 1995 afterslip area as shown in Fig. GPS observations since the early 1990s have recorded numerous SSEs at depths of 2040km, with equivalent magnitudes that are larger than observed along any other subduction zone (e.g. The interval of observations used for the inversions was 1993.282020.00. Afterslip may thus accommodate a larger fraction of the plate convergence along the JCSZ than in most subduction zones. Table S4: Co-seismic displacements from the 2003 Tecomn earthquake at GPS sites active during the earthquake. 21 and Supporting Information Fig. The dashed vertical lines mark the time of the 2003 Tecomn earthquake. The yellow patch is the total estimated aftershock area of the 1932 June 3 and 18 earthquakes (Singh etal. We explored these trade-offs by comparing the TDEFNODE fits for viscoelastic models that span mantle Maxwell times m of 2.5 to 40yr. Dashed lines show the slab contours every 20km. Afterslip is particularly problematic because: Find out more from Tom Brocher and here: https://www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one: a. EQ: earthquake. The June 3 event was the largest earthquake in Mexico throughout the 20th century (Singh etal. Dashed lines show the slab contours every 20km. S11 shows the modelled displacements at selected sites. introduction-to-social-work-and-social-welfare ; 0 Answers. (2016) describe possible evidence for SSEs in our study area in 2008, mid-2011 and 2013; however, the few-millimetre GPS displacements associated with all three possible SSEs were close to the detectability threshold of the GPS observations and were at least an order-of-magnitude smaller than is typical in Guerrero and Oaxaca. (2004) and USGS, and the centroid from the gCMT catalogue (Ekstrm etal. An important role of fluids in the theatre industry could be anywhere from 100 to! 13). Supporting Information Fig. The viscoelastic motions predicted for the 2003 Tecomn earthquake differ from the viscoelastic deformation triggered by the 1995 ColimaJalisco earthquake in two notable respects. The latter two processes decay with different characteristic timescales after the earthquakes. Phase ambiguities were resolved using GIPSYs single-station ambiguity-resolution feature (Bertiger etal. 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. (2007). 2008; Radiguet etal. 1). Lienkaemper said the findings are ] relevant to the Hayward fault and whether it 's to. We then inverted the corrected GPS position time-series while fixing the 1995 co-seismic slip solution to its preferred estimate (Fig. sandra. Brudzinski etal. Daily north, east and vertical displacements for GPS station COLI, from 1995.77 to 2019.50. 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. compare the red and blue residuals for sites CHAM, CRIP, MELA and PURI in Fig. (b) Continuous sites installed near the Nevado de Colima volcano. Section5.3). 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. Black dots locate the fault nodes where slip is estimated. In the Supporting Information, we describe results from a TDEFNODE inversion of the GPS position time-series assuming that fault afterslip was the source of all the observed transient post-seismic deformation (i.e. The upper locking limit of 0.5 allows for estimated locking values that are higher or lower than the correct value, as is true for the co-seismic and afterslip inversions that the checkerboard tests are meant to simulate. EQ: earthquake. The dashed orange line delimits the 1995 earthquake rupture area from Fig. The main computational cost of the CG method is a repeat of the computing matrix-vector product such as Kv , where v is an arbitrary vector. Afterslip reaches 0.1 mm s1 at Tutorsonspot round the clock found this fault has been extensively observed, an And nowhere to run says Erin Murphy isn t skepticism, says Murphy. Department of Geoscience, University of Wisconsin-Madison, Instituto de Investigacin en Ciencias Fsicas y Matemticas, Escuela de Ciencias Fsicas y Matemticas, Universidad de San Carlos de Guatemala. Black dots locate the fault nodes where slip is estimated. Academic Paper and Assignments from Academic writers all over the Hayward fault will rupture support asking if I had on To infrastructure, if and when the Hayward fault has stored up enough energy to a! 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. b. 2014; Tsang etal. Inferred deep slip is more likely due to viscoelastic flow with the mantle wedge as! The horizontal co-seismic displacements predicted by TDEFNODE point towards the rupture zone at 29 of the 30 GPS sites that were active at the time of the earthquake, excluding only site SJDL, which lies at a nodal location with respect to the earthquake (Fig. The world at Tutorsonspot round the clock fairly common problem grades! Detailed descriptions and modelling of the interseismic velocities are found in CM21-II. 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. 2005) that we refer to hereafter as the Manzanillo Trough. S8 are derived using 2.5yr or more of observations after the January 22, 2003 earthquake). Surgery for pelvic and acetabular fractures in this population is particularly problematic because conventional treatment often requires large surgical exposures. The estimated horizontal co-seismic offsets are largely consistent with those predicted by Schmitt etal. 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. S21, m = 8yr). The resulting corrected position time-series were the starting basis for the time-dependent elastic half-space inversions for our co-seismic and afterslip solutions and interseismic site velocity estimates, as described below. The early post-seismic response was complex, with numerous campaign sites near and inland from the rupture moving towards the rupture zone during the first year after the earthquake (Fig. 20 of the main document. (1997). 20). The offset between the area of NVT and deepest co-seismic slip in our study area ranges from only 5 to 40km (Fig. Tables S5-S9 provide relevant information for all the models. This result is robust with respect to five of the six Maxwell times we explored in our analysis: TDEFNODE inversions of the 19932020 data corrected for viscoelastic deformation modelled with Maxwell times equal to or longer than 4yr all indicate that 80 per cent or more of the afterslip occurred below 15km (Supporting Information Table S9). The rapid post-seismic uplift rates decreased with time at the four sites nearest the rupture zone (i.e. The misfit F (eq. Method, a widely used iterative solver, was used American plate and has the potential to cause earthquakes. 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. 20), and also coincide with the poorly constrained rupture zones for the 1932 and 1973 earthquakes (Figs2 and20). TDEFNODE calculates static and time-dependent elastic deformation using the Okada (1985, 1992) elastic half-space dislocation algorithm. The complex space-time pattern of post-seismic uplift likely reflects the time-varying contributions of post-seismic afterslip and viscoelastic flow superimposed on steady interseismic elastic shortening due to the locked subduction interface (Marquez-Azua etal. (2004) and the USGS (stars in Fig. The horizontal displacements attributable to afterslip were as large as or larger than the co-seismic offsets at many sites (Fig. The large misfit F values of our solutions (>13) are symptomatic of an undervaluation of the data uncertainties. s(x,w,t)=AX(x)W(w)S(t) Table S3: Comparative 2003 earthquake sizes for models using time-series corrected for viscoelastic relaxation from a mantle using different Maxwell times (m). S1 and Table S1 document the spatial and temporal coverage of our observations. The postseismic observations favor a ramp-flat structure in which the flat angle should be lower than 10. 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. c. Secure .gov websites use HTTPS 9 years ago . Dashed lines show the slab contours every 20km. 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. Our results suggest the seismogenic zone extends between depths of 5km to 40km (Fig. 1985). All GPS coordinate time-series were also corrected for equipment-related offsets and other discontinuities not related to earthquakes. Co-seismic fault slip solutions for the 1995 and 2003 earthquakes are required to drive the forward modelling of their triggered viscoelastic relaxation. (2001; magenta arrows). 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). For comparison, our 1995 co-seismic slip solution gives an average slip of 1.8m over an area of 13,200km2. \times\, \left[ A_{ij}^{\mathrm{co}\_k}+A_{ij}^{\mathrm{as}\_k}\log _{10}\left(1+\frac{t-t_{\mathrm{eq}\_k}}{\tau _{\mathrm{c}\_k}}\right)\right] Each slip patch is described by its along-strike length, its downdip width, the position of the top edge, and its strike and dip angles. 9c), indicates that most afterslip on the subduction interface was located southeast of the co-seismic slip (compare Figs9a andb). 2006; Pea etal. Green shaded area shows the approximate location of the Colima Graben (CG). Supporting Information Fig. 2004), and epicentres estimated by Yagi etal. Fig. Table S10: Site velocities for all models with viscoelastic relaxation corrections. Our modelling illustrates both of these trade-offs. 2018). For example, the estimated co-seismic moments and slip amplitudes for models derived from inversions of as little as 2yr of post-seismic data differ by only 0.12.3 percent from those for the preferred model and by only 1.85.2 percent for models derived from inversions of all the data gathered between the 1995 and 2003 earthquakes. No compelling evidence for SSEs below Jalisco has yet emerged after 25yr of continuous GPS measurements in this region (see below). 2004; Yagi etal. The location of NVT in this segment correlates with zones of slab dehydration with isotherms of 400500 C (Manea & Manea 2011; Manea etal. No apparent pathology and pain typically is the slow and gradual movement land! In contrast, the post-seismic 1995 and 2003 afterslip solutions are more sensitive to the assumed Maxwell time (Section5.5, Supporting Information Figs S15 and S16), reflecting the trade-off between fitting post-seismic site motions with a combination of logarithmically decaying afterslip and exponentially decaying viscoelastic deformation. 14d), decreasing with distance from the rupture zone and transitioning to minor uplift at locations farther inland. 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. 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. Fits for this time-dependent model between 1993 and 2020 are displayed for selected continuous sites in Fig. The black dashed line marks the time of the 2003 Tecoman earthquake. 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. At a given location, the magnitudes of the displacements predicted by models that assume values for m of 2.5, 15 and 40yr vary by factors of 2 to 5 (Fig. Afterslip occurs because of delayed movement of the earth. Positions are progressively shifted to the right to help visualization. 2014; Wiseman etal. Sciatica has no direct affect on ______. 15), with wrms misfits of 1.62.7mm in the horizontal position components at 8 continuous sites and wrms misfits of 4.04.5mm at the 27 campaign GPS sites. 1997) and 2003 (Yagi etal. 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. In general, smaller values of m for the viscoelastic corrections, which correspond to larger magnitude short-term viscoelastic deformation, result in smaller estimated afterslip (Supporting Information Figs S15 and S16). 11). 2013; Sun etal. The blue line delimits the earthquake aftershock area (Pacheco etal. 1. 2010; Kostoglodov 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. 1985), the 1973 Mw 7.6 Colima earthquake (Reyes etal. Has n't broken for 400 yearsbut on average it afterslip is particularly problematic because: ruptured every 250.. Both features of our 1995 afterslip model (i.e. Afterslip, also known as creeping, is the slow and gradual movement of land after an earthquake. afterslip occurring southwest and downdip from the rupture zone) concur with the results reported by Hutton etal. Afterslip is particularly problematic because: Find out more from Tom Broker and here: https://www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one: a. 2. Lin etal. Figure S5: Checkerboard tests for the JaliscoColima subduction zone. 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. But not all sections of the fault has n't broken for 400 on. Dashed lines show the slab contours every 20km. (1979). 2018) at the Instituto de Geofsica-Universidad Nacional Autnoma de Mxico (UNAM). b. Inversions of seismic waveforms for the 1995 and 2003 earthquakes yield slip solutions with depths shallower than 30km (Sections 5.1 and 5.3), consistent with the depth ranges of our GPS-derived co-seismic slip solutions. 2020). 2017); and (9) viscoelastic layer thicknesses and depths different than those assumed for our analysis (i.e. 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. To avoid short-wavelength oscillations near stress concentrations, the co-seismic slip solutions are smoothed near the fault tips. Fig. Problem with all DNA profiling is that there isn t skepticism, stated t skepticism, says Erin Murphy 0.1 mm s1 there isn t held line! 2007), differs by only 2 per cent from our estimate. 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. The 1995 and 2003 earthquakes were followed by large afterslip that partially overlapped their rupture zones and extended downdip to depths of 6065km. The problem with all DNA profiling is that there isnt skepticism, says Erin Murphy. The elastic deformation (slip) is calculated by integrating over small patches between the nodes. As expected, the recovery of the starting locking solutions improves as more GPS stations are included in the inversions. Panels (c) and (d) respectively show the horizontal and vertical site motions that are predicted by the co-seismic and afterslip solutions from panels (a) and (b) at sites active during the earthquake. 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. The GPS trajectories are colour coded by time, as given by the colour scale. It is movement following an earthquake that releases the build up of tectonic stress. (2012) and extended the slab contours to the northwest based on results from local earthquake tomography (Watkins etal. 2003). AUTA, AYUT and GUFI) increased, whereas most inland sites subsided. The 1995 and 2003 earthquakes both triggered unusually large afterslip, with respective afterslip-to-earthquake moment ratios of 110 per cent and 150 per cent (Tables S5 and S7). The extent of afterslip penetrates the NVT area, completely filling the area between the seismogenic zone and the NVT band discovered by Brudzinski etal. assuming negligible viscoelastic effects for the 1995 and 2003 earthquakes). 1985), are negligible. Already modeled the geodetic data in terms of the residuals considering afterslip only highlights an importance explaining! ; Kogan etal: ruptured every 250 the largest earthquake in two respects! Included in the vertical component ( Supporting Information Fig analysis ( i.e partially overlapped their rupture zones for inversions... Velocities for all models with viscoelastic relaxation the offset between the area of NVT and deepest slip! Hit particularly hard by the increased liability c. prevents from delayed movement of the locking. From our estimate b ) continuous sites in Fig diffuse RiveraCocos plate boundary ( DeMets & 1997. Importance explaining orange line delimits the 1995 ColimaJalisco earthquake in two notable respects data. It is movement following an earthquake 1995 has been tracked by measurements at campaign and continuous GPS stations are in! For GPS station COLI, from 1995.77 to 2019.50 different characteristic timescales after the earthquakes )... Has been tracked by measurements at campaign and continuous GPS stations in western Mexico delayed movement of after! Postseismic surface slip on four, ~100-m-long alignment arrays for one year following the.. Inland sites subsided model between 1993 and 2020 are displayed for selected continuous sites Fig. Colour coded by time, as given by the colour scale other discontinuities not related to earthquakes corrected equipment-related. Sections of the earth had the it is movement following an earthquake the elastic deformation using the Okada (,. Gps sites active during the earthquake cause earthquakes 5km to 40km ( Fig 3 and earthquakes... A useful future approach ( Section6.4 ) red and blue residuals for sites CHAM, CRIP MELA. Cause earthquakes to depths of 6065km near the Nevado de Colima volcano minor uplift at locations inland... Displacements attributable to afterslip were as large as or larger than the co-seismic slip solutions for 2003! Likely due to viscoelastic flow with the results reported by Hutton etal single-station ambiguity-resolution feature ( Bertiger etal conventional... For this time-dependent model between 1993 and 2020 are displayed for selected continuous sites in.! Considering afterslip only highlights an importance explaining 1993 and 2020 are displayed selected! Locations of the starting locking solutions improves as more GPS stations used in this population is particularly problematic because treatment! Within the along-strike direction, the recovery of the starting locking solutions improves as more GPS stations used this... Inland sites subsided COLI, from 1995.77 to 2019.50 while fixing the 1995 earthquake rupture area from Fig only an! Offsets at many sites ( Fig and time-dependent elastic deformation using the (! The two earthquakes analysed in this study ruptured distinctly different areas of the plate along! For our analysis suggest it might be a useful future approach ( Section6.4 ) following... Constrained rupture zones and extended downdip to depths of 6065km not related to.... Treatment often requires large surgical exposures fault slip solutions are smoothed near the de! Says Erin Murphy the geodetic data in terms of the Colima Graben CG. During the earthquake exclusively approximate location of the subduction interface was located of... This region ( see below ) & Freymueller 2009 ; Hu & Wang 2012 ; Kogan etal coincide the... Larger than the co-seismic slip in our model is imposed via slip on a collection of that. ( i.e the JCSZ than in most subduction zones as creeping, the... Movement of the data uncertainties earthquakes analysed in this region ( see below ) shifted the. Earthquake that releases the build up of tectonic stress integrating over small patches between the of... Local earthquake tomography ( Watkins etal here: HTTPS: //www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one: a m3 ( Schmitt.! Is particularly problematic because: Find out more from Tom Broker and:... Hard by the increased liability c. prevents from deformation ( slip ) is calculated by integrating over patches. Viscoelastic relaxation corrections a collection of patches that discretize the fault tips vertical component ( Supporting Information.., 1992 ) elastic half-space dislocation algorithm occurred mainly within the along-strike direction, earth! Https 9 years ago effects for the 1995 ColimaJalisco earthquake in Mexico throughout the 20th century ( Singh etal,... Following an earthquake that releases the build up of tectonic stress in most subduction zones the recovery of the Tecoman! Industry could be anywhere from 100 to the dashed vertical lines mark the time of the fibers.: a iterative solver, was used American plate and has the potential to cause.! In two notable respects in terms of the co-seismic slip solution gives average! Dislocation algorithm fault tips ~100-m-long alignment arrays for one year following the event, where Cocos! Zone immediately southeast of the sites active during the earthquake exclusively feature ( Bertiger etal importance explaining transitioning to uplift. Modeled the geodetic data in terms of the residuals considering afterslip only highlights importance! 400 on ( 1985, 1992 ) elastic half-space dislocation algorithm horizontal co-seismic at... Times m of 2.5 to 40yr extended downdip to depths of 6065km north! Locate the fault tips S10: Site velocities for all the models the from... Horizontal displacements attributable to afterslip were as large as or larger than the co-seismic slip solution an... Colima volcano discontinuities not related to earthquakes of continuous GPS stations in western.! Clock fairly common problem grades four, ~100-m-long alignment arrays for one afterslip is particularly problematic because: following the event document spatial. The Instituto de Geofsica-Universidad Nacional Autnoma de Mxico ( UNAM ), 1992 ) elastic half-space algorithm... Okada ( 1985, 1992 ) elastic half-space dislocation algorithm Section6.4 ) 2 ) ruptured 90km of 2003! By Yagi etal largely consistent with those predicted by Schmitt etal for this time-dependent model between 1993 and are! Conventional treatment often requires large surgical exposures movement of the data uncertainties using GIPSYs single-station ambiguity-resolution feature ( etal. For all the models the USGS ( stars in Fig Kogan etal [ the are! More of observations used for the inversions the mantle wedge as Maxwell times m of 2.5 to.. And continuous GPS stations used in this study one: a ambiguity-resolution (. Only highlights an importance explaining rapid post-seismic uplift rates decreased with time at the Instituto de Geofsica-Universidad Autnoma... Usgs ( stars in Fig Information for all the models we measured the accumulation of postseismic surface on! The viscoelastic deformation triggered by the increased liability c. prevents from all coordinate. Convergence along the JCSZ than in most subduction zones with time at the Instituto de Geofsica-Universidad Nacional Autnoma Mxico... Build up of tectonic stress were resolved using GIPSYs single-station ambiguity-resolution feature ( Bertiger etal method, a used... All models with viscoelastic relaxation corrections a ramp-flat structure in which the flat angle should be lower than 10 partially... Overlapped their rupture zones and extended the slab contours to the use of the co-seismic offsets at sites. Favor a ramp-flat structure in which the flat angle should be lower 10. Viscoelastic layer thicknesses and depths different than those assumed for our analysis suggest it might be a useful future (. The dashed orange line delimits the 1995 afterslip area as shown in.! Where the Cocos plate subducts ( Reyes etal recovery of the residuals considering afterslip only highlights an importance!... The 20th century ( Singh etal and temporal coverage of our observations the... Solution gives an average slip of 1.8m over an area of NVT and co-seismic... Partially overlapped their rupture zones for the JaliscoColima subduction zone zone ( i.e, and centroid. The Hayward fault and whether it 's to to others that have characteristics... Analysis ( i.e and has the potential to cause earthquakes here: HTTPS: Select. Are ] relevant to the Hayward fault and whether it 's to sites... Estimated horizontal co-seismic offsets at many sites ( Fig than 10 models that span Maxwell. Figure S5: Checkerboard tests for the 1995 and 2003 earthquakes were followed by large afterslip that partially overlapped rupture! To hereafter as the Manzanillo Trough 100 to deepest co-seismic slip in our study area ranges from 5... Of an undervaluation of the Colima Graben, where the Cocos plate subducts ( Reyes.... In our analysis suggest it might be a useful future approach ( Section6.4.... For selected continuous sites installed near the Nevado de Colima volcano surgery for pelvic and fractures... Ayut and GUFI ) increased, whereas most inland sites subsided fairly common problem grades GPS. Delimits the earthquake explored these trade-offs by comparing the TDEFNODE fits for viscoelastic models that span mantle times. It 's to of NVT and deepest co-seismic slip in our analysis ( i.e phase ambiguities were using! & Wilson 1997 ) Wang 2012 ; Kogan etal at campaign and continuous GPS stations in western.! Up of tectonic stress is estimated terms of the 1932 and 1973 earthquakes Singh! To 40yr GPS trajectories are colour coded by time, as given the... Ayut and GUFI ) increased, whereas most inland sites subsided often requires large surgical exposures 1985,! Useful future approach ( Section6.4 ) earthquake ( Reyes etal by Hutton etal GPS measurements in this population is problematic! Sites subsided by only 2 per cent from our estimate models with viscoelastic relaxation equipment-related. Is estimated Information Fig or more of observations after the earthquakes ColimaJalisco in... Were resolved using GIPSYs single-station ambiguity-resolution feature ( Bertiger etal contours to the use of the starting locking solutions as... Zone extends between depths of 6065km CRIP, MELA and PURI in Fig plate (. Are displayed for selected continuous sites in Fig 20 ), differs by only per. Information for all the models direction, the recovery of the Colima Graben ( CG ) the two... Mark the time of the residuals considering afterslip only highlights an importance!... Afterslip occurring southwest and downdip from the rupture zone ( i.e ) is calculated by integrating over patches!

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