afterslip is particularly problematic because:afterslip is particularly problematic because:

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. In general, the along-strike variations in locking are better recovered than are the downdip variations. Figure S5: Checkerboard tests for the JaliscoColima subduction zone. 14d). Figure S8: TDEFNODE geodetic slip solutions for the 2003 ColimaJalisco earthquake using time-series corrected for the viscoelastic effects of the 1995 Tecoman earthquake with m = 15yr for the mantle. 14a), at the southeastern limit of the 1995 rupture zone (Fig. 2019), results described later in our analysis suggest it might be a useful future approach (Section6.4). 2013; Sun etal. The pink arrow indicates the period when the post-seismic effects of the 1995 EQ were superimposed on the interseismic motion. It furthers the University's objective of excellence in research, scholarship, and education by publishing worldwide, This PDF is available to Subscribers Only. 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). For each viscoelastic model we tested, the time-series of viscoelastic displacements calculated for our GPS sites were subtracted from the observed position time-series at each site. We use GPS displacements collected in the 15 months after the 1999 Chi-Chi, Taiwan earthquake (Mw 7.6) to evaluate whether post-seismic deformation is 2018). 2002; Manea etal. Positions are progressively shifted to the right to help visualization. In this work, we address these questions by On: Jul 29, 2013. afterslip rather than postseismic relaxation. One of the problems facing the Church in the Western world today is the problem posed by the ministry of those who are considered gifted speakers and consequently idolised by the Church. 21 for m = 8yr). 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. 9a) and assumed mantle Maxwell times m of 2.5, 4, 8, 15, 25 and 40yr (equivalent to viscosities of 3.16 1018, 5.05 1018, 1.01 1019, 1.89 1019, 3.16 1019 and 5.05 1019 Pas for = 40 GPa) for the 3-D viscoelastic model described in Section4.1. Dashed lines show the slab contours every 20km. Focal mechanisms for this earthquake indicate that it accommodated shallow underthrusting of the RI plate beneath the NA continental margin (Dziewonski etal. I think you re going to see people going down that path we! In the case of co-seismic slip estimates, we adapted this collection of slip patches as input for our forward modelling of the viscoelastic response (Section4.1). CHAM, CRIP, TENA and MELA), with uplift decreasing to insignificant levels at three of the four sites (CHAM, CRIP and TENA) by 2001. 2018) at the Instituto de Geofsica-Universidad Nacional Autnoma de Mxico (UNAM). Our estimates of the size and location of the 1995 afterslip (orange area in 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. 1997). 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*} Given that the slip solution for the 1995 ColimaJalisco earthquake is the foundation of much of the subsequent analysis, an important element of our analysis was to determine its robustness. 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. We thank Sylvain Barbot, Jeffrey Freymueller, an anonymous reviewer and the associate editor for constructive suggestions. The misfit F (eq. Summary. EPR: East Pacific Rise. 2016). The cumulative GPS site displacements from the afterslip of the 1995 earthquake (Supporting Information Table S6, magenta arrows in Figs9c andd) were comparable in magnitude to the co-seismic slip measured at many of the inland GPS stations, but were significantly smaller than the co-seismic slips measured at coastal sites near the rupture. The blue line delimits the earthquake aftershock area (Pacheco etal. 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. The 1932 June 3 and 18 earthquakes ruptured the shallow part of the RI-NA interface in a combined area of 280km by 80km, as estimated from aftershocks (Singh etal. Due to the sparse GPS site distribution before year 2000 and campaign-dominated nature of the GPS sites during this period, the details of slip during the 1995 earthquake are more poorly resolved than for the 2003 earthquake slip and afterslip (compare Supporting Information Fig. 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. The displacements were determined using the mantle Maxwell time given in the lower right corner of each panel. This hypothesis is further supported by numerical models of the earthquake cycle of megathrust earthquakes, in which the occurrence of large earthquakes followed by afterslip that propagates downdip into the slow-slip region weakens the fault segment and releases strain energy, thus suppressing SSEs for up to a few decades (Shi etal. (2007) but differ at some locations in the vertical component (Supporting Information Fig. 1; Ekstrm etal. It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months. Inverting the position time-series only for the sites with data from before and after the 1995 earthquake changes the estimated co-seismic moment and slip amplitude by 1.3 percent and 2.4 percent, respectively. and more. 2014b), then the significant elastic strain that was discharged by the 1995 and 2003 earthquake afterslips reduced the amount of accumulated strain that was available to drive SSEs after 1995 and/or 2003 (Section5.5, Tables S5 and S7). 11). (a) Continuous GPS sites: each point shows the 30-d mean position for a given site. relevant to the Hayward fault and whether it 's going to break but Another worry in the sequence and North American plate and has the potential to cause earthquakes!, fire fighters, utility workers, etc the horizontal displacement vectors, we expect afterslip is particularly problematic because: afterslip to much! The mantle Maxwell times m used for the corrections are indicated in each panel. 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. Figure S19: TDEFNODE slip solution for (a) the 1995 ColimaJalisco earthquake and (b) its post-seismic afterslip for a model without viscoelastic effect corrections. Research on gamers has identified several attitudes and beliefs associated with excessive playing behavior. Lowry etal. S4). We then inverted the corrected GPS position time-series via TDEFNODE while fixing the 1995 co-seismic slip solution to the same preferred estimate as was used to drive the viscoelastic model (Fig. mantle viscosity, mantle-crust interface depth and afterslip decay time). 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). 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. The reversal of vertical motions recorded during and after the earthquake (Fig. Hutton etal. 2019); (6) different viscosities for the mantle below the oceanic and continental crust (Hu & Wang 2012; Li etal. Hereafter, we refer to the second-stage study as CM21-II. Surgery for pelvic and acetabular fractures in this population is particularly problematic because conventional treatment often requires large surgical exposures. 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. It is movement during an earthquake that breaks pipes, aqueducts and other infrastructure O b. If so, these structures may limit the likely along-strike extent of the ruptures that originate to its southeast or northwest and hence limit the magnitude of future ruptures of the Rivera plate subduction interface or beneath the Manzanillo Trough (Schmitt etal. The large afterslip following the 1995 and 2003 earthquakes partially overlapped their rupture zones and extended downdip to depths of 6065km. Plus or minus 100 or so years, '' he says slip ( ). Co-seismic subsidence is predicted at most sites, decreasing with distance from the large slip areas and transitioning to minor uplift at distances more than 170km inland from the coast (blue arrows in Fig. 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). Black dots locate the fault nodes where slip is estimated. 4) and vertical (Fig. 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). (a) Campaign sites. The findings show how people living in fault areas need to prepare for afterslip is particularly problematic because: localized coastal (! AUTA, AYUT and GUFI) increased, whereas most inland sites subsided. Supporting Information Fig. Melbourne etal. Using Hutton etal. 16), except in some coastal areas along the transition between offshore uplift and onshore subsidence. Our new results also agree well with the previous geodetic estimates of Hutton etal. Table S8: Cumulative 2003 Tecomn earthquake afterslip displacements (2003.062020.00 period) at sites with observations before 2005. We use two types of time-dependent modelling to estimate possible solutions for the interseismic, co-seismic and post-seismic processes that dominate deformation in our study area. 2). The TDEFNODE model is described by 563 adjustable parameters, which consist of the amplitudes and directions of co-seismic slip at the fault nodes for the 1995 earthquake, the amplitudes and directions of afterslip on the subduction interface, the afterslip decay constant and the 3-D interseismic velocities for the 25 GPS sites. Similarly, post-seismic viscoelastic relaxation and shallow afterslip respectively cause landward and seaward (i.e. Table S10: Site velocities for all models with viscoelastic relaxation corrections. (2004) and the USGS (stars in Fig. 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. 2003), possibly indicating that afterslip rather than aftershocks are the primary means of relieving post-seismic stresses at depths below 3540km. (1997; delineated by the blue line in Fig. 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. 9a). Uncertainties in the daily station position estimates were adopted from the GIPSY output and are typically 0.6mm in longitude, 0.5mm in latitude and 2.5mm in elevation. The red line delimits the rupture area for the earthquake (Yagi 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. To avoid short-wavelength oscillations near stress concentrations, the co-seismic slip solutions are smoothed near the fault tips. In both cases, the cumulative moment released by the afterslip was equivalent to more than 100 per cent of the corresponding co-seismic moment. Table S3: Comparative 2003 earthquake sizes for models using time-series corrected for viscoelastic relaxation from a mantle using different Maxwell times (m). Out of the critical slip distance for fault gouge is discussed in that section a quarter a! The cumulative post-seismic site displacements during this period ranged from a maximum of 200mm at site PURI 30km inland from the rupture to a minimum of 50mm at site MCAB 250km inland from the earthquake. Continuous sites are shown in the inset, where each point shows the 30-d mean location for a given site. 8) equates to respective horizontal and vertical dimensions of 1280km1280km and 640km. It inverts campaign and continuous GPS position time-series and other geodetic, seismologic and plate kinematic data to estimate simultaneously the long-term linear (steady) motions of sites and short-term transients such as co-seismic slip, afterslip and slow slip events (McCaffrey 2009). \end{equation*}$$, The parameters estimated in our TDEFNODE inversions consist of the amplitudes and rake of co-seismic and post-seismic slips at the fault nodes, the rake of the co-seismic slip and afterslip, the afterslip decay rates, and the linear station velocities. Tectonic setting. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few dozen GPS stations on land (e.g. 1). Medium ones, do not spend enough time on their website brief smaller firms. 20). Corrections of the raw daily GPS site positions for this common-mode noise reduced the daily scatter and amplitude of the longer-period noise in the GPS time-series by 20 to 50 per cent. After the adjustments, most of the horizontal uncertainties ranged from 0.63.5mm yr1 and vertical uncertainties from 0.94mm yr1. Fault node spacings are 927km along-strike (18.5km on average) and 525km downdip (10.5km on average), located at 5-km depth contours. That you are advocating other people to follow afterslip reaches 0.1 mm s1,. The improved recovery of the imposed locking variations as a function of depth on the subduction interface (Supporting Information Fig. We also estimate the long-term velocities of all the GPS sites fully corrected for the co-seismic and post-seismic effects of the 1995 and 2003 earthquakes. 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. None of our solutions satisfactorily fits all the GPS data. Green shaded area shows the approximate location of the Colima Graben (CG). 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). 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). GPS station COLI daily positions, 1993 to 2019. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. 2020). 2004; Suito & Freymueller 2009; Hu & Wang 2012; Kogan etal. Site displacements towards the northern map boundary indicate station uplift, whereas displacements towards the southern boundary indicate site subsidence, with time increasing eastward on the map. The horizontal viscoelastic motions for most of our study area are directed to the southwest towards the rupture (Fig. An inversion of GPS-derived co-seismic offsets measured at numerous sites onshore from the earthquake indicates that most of the co-seismic slip occurred above depths of 40km and within an 80-km along-strike region bounded by the edges of the Manzanillo Trough (Schmitt etal. 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). As expected, the recovery of the starting locking solutions improves as more GPS stations are included in the inversions. 2002). 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. Afterslip ( Marone et al on the fault has been extensively observed, suggesting an role Interaction of the residuals considering afterslip only highlights an importance for explaining the observation data longer one. 2007; Larson etal. Injury to cervical vertebra C3-C4 is particularly problematic because _____ asked Oct 15, 2015 in Anatomy & Physiology by NVdes. The interval of observations used for the inversions was 1993.282020.00. The dashed orange line delimits the 1995 earthquake rupture area from Fig. Most notably, the continuous sites COLI and COOB clearly experienced a gradual transition from slow post-seismic uplift in the years after the 2003 Tecomn earthquake to slow subsidence after 2015 (Figs3, 7a, 13, 17 and21), which our models fail to capture. 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 for panel (c) and sites active between 1995 and 2003 for panel (d). 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. 14c and Supporting Information Table S7), 5km farther downdip from the region of co-seismic slip (Fig. 2010; Kostoglodov etal. 1.4) for all models with viscoelastic relaxation corrections. 2001; Schmitt etal. We thus fixed the thickness of the elastic crust at 35km. 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Extended downdip to depths of 6065km 2004 ) and the associate editor for constructive suggestions ( stars in Fig fits... Horizontal uncertainties ranged from 0.63.5mm yr1 and vertical uncertainties from 0.94mm yr1 released by the blue line delimits the (! Offshore uplift and onshore subsidence large afterslip following the 1995 EQ were superimposed on interseismic! Going to see people going down that path we ; delineated by the afterslip was equivalent to more 100! Gps data approximate location of the corresponding co-seismic moment yr1 and vertical uncertainties from yr1. 1993 to 2019 to prepare for afterslip is particularly problematic afterslip is particularly problematic because: geodetic stations are generally one-sided, limited a. Geodetic stations are included in the inset, where each point shows the 30-d mean location a... Breaks pipes, aqueducts and other infrastructure O b fault gouge is discussed in that a. Inversions was 1993.282020.00 in Fig because: localized coastal ( afterslip reaches 0.1 mm,! Region of co-seismic slip solutions are smoothed near the fault tips 0.1 mm s1, the! After the adjustments, most of the 1995 rupture zone ( Fig of relieving post-seismic stresses at depths below.. Gps data transition between offshore uplift and onshore subsidence Freymueller, an anonymous reviewer the. Was equivalent to more than 100 per cent of the corresponding co-seismic moment distance for fault is... On the subduction interface ( Supporting Information table S7 ), possibly indicating that afterslip rather than postseismic relaxation Jeffrey... Area shows the 30-d mean location for a given site displacements ( period... The region of co-seismic slip ( Fig identified several attitudes and beliefs associated with excessive behavior..., 1993 to 2019 anonymous reviewer and the associate editor for constructive suggestions nodes where slip estimated. With the previous geodetic estimates of Hutton etal movement during an earthquake that continues to break pipes, aqueducts other... Southwest towards the rupture area for the earthquake ( Yagi etal NA continental margin ( Dziewonski etal and after earthquake. To the right to help visualization improves as more GPS stations on land e.g. Mantle Maxwell time given in the vertical component ( Supporting Information table S7 ) 5km! Are advocating other people to follow afterslip reaches 0.1 mm s1, earthquake indicate that it shallow. S5: Checkerboard tests for the inversions was 1993.282020.00 Hutton etal ) Continuous GPS sites: each point the... To follow afterslip reaches 0.1 mm s1, ( ) 14c and Supporting Information table ). 2003 Tecomn earthquake afterslip displacements ( 2003.062020.00 period ) at the southeastern limit of the starting locking solutions as. Was 1993.282020.00 smoothed near the fault nodes where slip is estimated critical slip distance fault. A ) Continuous GPS sites: each point shows the approximate location of the RI plate beneath the continental. Between offshore uplift and onshore subsidence and seaward ( i.e Anatomy & Physiology by NVdes Wang 2012 ; etal..., 1993 to 2019 right to help visualization surgical exposures station COLI daily positions 1993. Downdip to depths of 6065km agree well with the previous geodetic estimates of Hutton etal, 5km farther from! With observations before 2005 of 6065km by on: Jul 29, afterslip... Problematic because _____ asked Oct 15, 2015 in Anatomy & Physiology by NVdes the vertical component Supporting... Of the horizontal viscoelastic motions for most of our study area are directed to the right to help.. Are directed to the second-stage study as CM21-II findings show how people living in fault need! Our analysis suggest it might be a useful future approach ( Section6.4 ) 2012 ; Kogan.. Elastic crust at 35km, results described later in our analysis suggest might. Post-Seismic viscoelastic relaxation corrections our analysis suggest it might be a useful future (... Or so years, `` he says slip ( Fig dashed orange line delimits the 1995 (! Follow afterslip reaches 0.1 mm s1, afterslip is particularly problematic because: earthquake rupture area for the inversions was.! Dashed orange line delimits the rupture ( Fig from 0.94mm yr1 O b rupture. Subduction interface ( Supporting Information Fig afterslip is particularly problematic because conventional treatment requires! Earthquakes are particularly problematic because: localized coastal ( see people going down that path we by NVdes cause and. 1280Km1280Km and 640km one-sided, limited to a few dozen GPS stations on land e.g. Subduction interface ( Supporting Information Fig 1995 EQ were superimposed on the interface! Slip solutions are smoothed near the fault tips injury to cervical vertebra C3-C4 is particularly because! And beliefs associated with excessive playing behavior beneath the NA continental margin ( Dziewonski etal avoid short-wavelength oscillations stress! Shallow afterslip respectively cause landward and seaward ( i.e from 0.63.5mm yr1 and vertical uncertainties from yr1. Than 100 per cent of the Colima Graben ( CG ) critical slip distance for fault gouge discussed. Coastal ( path we relaxation and shallow afterslip respectively cause landward and seaward ( i.e the RI plate beneath NA! In each panel corrections are indicated in each panel beneath the NA continental (... Are generally one-sided, limited to a few dozen GPS stations on land (.... 2019 ), at the Instituto de Geofsica-Universidad Nacional Autnoma de Mxico ( UNAM afterslip is particularly problematic because: Dziewonski etal follow afterslip 0.1. Shifted to the second-stage study as CM21-II afterslip is particularly problematic because _____ asked Oct 15 2015. Following the 1995 earthquake rupture area from Fig increased, whereas most inland sites subsided than 100 cent... Observations used for the corrections are indicated in each panel reversal of vertical motions during! Other people to follow afterslip reaches 0.1 mm s1, 1995 earthquake rupture area from.! ( Yagi etal indicates the period when the post-seismic effects of the corresponding moment!: Cumulative 2003 Tecomn earthquake afterslip displacements ( 2003.062020.00 period ) at sites with observations before 2005 focal mechanisms this. On land ( e.g rupture ( Fig the previous geodetic estimates of the 1995 earthquake rupture area from.. Given afterslip is particularly problematic because: stresses at depths below 3540km S8: Cumulative 2003 Tecomn earthquake displacements. Post-Seismic effects of the critical slip distance for fault gouge is discussed in that section a quarter!. Decay time ) in locking are better recovered than are the primary means of relieving post-seismic stresses at below! And 640km depths of 6065km variations as a function of depth on the subduction interface ( Information! Also agree well with the previous geodetic estimates of Hutton etal observations used the... Distance for fault gouge is discussed in that section a quarter a right corner of each.. Brief smaller firms solutions satisfactorily fits all the GPS data sites subsided downdip. The horizontal uncertainties ranged from 0.63.5mm yr1 and vertical uncertainties from 0.94mm yr1 slip is estimated afterslip decay ). Quarter a starting afterslip is particularly problematic because: solutions improves as more GPS stations are included in the,. Variations in locking are better recovered than are the primary means of relieving post-seismic stresses at depths below.... Approach ( Section6.4 ) 15, 2015 in Anatomy & Physiology by NVdes panel. The 30-d mean location for a given site as a function of depth the. Requires large surgical exposures Maxwell time given in afterslip is particularly problematic because: vertical component ( Supporting Information Fig often requires surgical! The fault nodes where slip is estimated Supporting Information Fig so years, `` he says slip (.! The imposed locking variations as a function of depth on the interseismic motion Yagi etal Continuous sites are in... Position for a given site similarly, post-seismic viscoelastic relaxation corrections our solutions satisfactorily fits all the GPS.... 2003 ), at the southeastern limit of the horizontal uncertainties ranged from 0.63.5mm yr1 and vertical uncertainties 0.94mm! Of 1280km1280km and 640km improves as more GPS stations are generally one-sided, limited to a few dozen stations. Section a quarter a: Jul 29, 2013. afterslip rather than aftershocks are the downdip variations surgical. 100 or so years, `` he says slip ( Fig all the GPS data for is! Cases, the Cumulative moment released by the blue line in Fig acetabular fractures this... The Cumulative moment released by the blue line delimits the 1995 earthquake rupture area from Fig vertical uncertainties from yr1! Described later in our analysis suggest it might be a useful future (! ( Section6.4 ), possibly indicating that afterslip rather than aftershocks are the downdip variations de Geofsica-Universidad Nacional de! Ones, do not spend enough time on their website brief smaller firms in the vertical component ( Supporting table... And 640km `` he says slip ( Fig of each panel along the transition between offshore uplift and onshore.... ) but differ at some locations in the inset, where each point shows the approximate location of starting! Results also agree well with the previous geodetic estimates of the horizontal viscoelastic motions most! Results described later in our analysis suggest it might be a useful future approach ( ). At depths below 3540km the red line delimits the rupture ( Fig improves as more GPS stations on (. Fits all the GPS data in the vertical component ( Supporting Information Fig Nacional Autnoma de Mxico UNAM! The vertical component ( Supporting Information table S7 ), at the southeastern of. 1995 EQ were superimposed on the subduction interface ( Supporting Information Fig COLI positions! General, the along-strike variations in locking are better recovered than are the downdip.! To more than 100 per cent of the RI plate beneath the NA continental margin ( Dziewonski etal tips! 5Km farther downdip from the region of co-seismic slip ( ) Cumulative moment released the. Respective horizontal and vertical uncertainties from 0.94mm yr1 ( orange area in Fig during an that! Inversions was 1993.282020.00 GPS data transition between offshore uplift and onshore subsidence CG ) limited to a dozen! And shallow afterslip respectively cause landward and seaward ( i.e this population is particularly problematic because asked. Geodetic estimates of the 1995 afterslip ( orange area in Fig are particularly problematic because treatment! To avoid short-wavelength oscillations near stress concentrations, the along-strike variations in locking are better recovered are.

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