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). 2014; Freed etal. Bottom right panel (1993.282020.00) corresponds to a model with no viscoelastic corrections. No previous afterslip solution for this earthquake has been estimated, although Schmitt etal. 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), using daily seven-parameter Helmert transformations from the JPL. mantle viscosity, mantle-crust interface depth and afterslip decay time). 2016). In this first part of a two-part study, we estimate geodetic co-seismic slip and post-seismic afterslip solutions for the 1995 ColimaJalisco and 2003 Tecomn earthquakes via time-dependent modelling of 1993-to-2020 GPS daily station positions from the state of Jalisco and neighbouring states, including calibrations for the viscoelastic rebound triggered by these events. (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski etal. 16) includes uplift immediately onshore from the rupture zone and in areas farther inland, but subsidence in most other regions. Okay, internet. UNAVCOs initial support for TLALOCNet (now part of NOTA) was performed under EAR-1338091 and is currently supported by the National Science Foundation and the National Aeronautics and Space Administration under NSF Cooperative Agreement EAR-1724794. 2020). The findings show how people living in fault areas need to prepare for afterslip is particularly problematic because: localized coastal (! Afterslip thus appears to relieve significant stress along the Rivera plate subduction interface, including the area of the interface between a region of deep non-volcanic tremor and the shallower seismogenic zone. Black dots locate the fault nodes where slip is estimated. 2004; Fig. We invert 25yr of campaign and continuous Global Positioning System daily positions at 62 sites in southwestern Mexico to estimate co-seismic and post-seismic afterslip solutions for the 1995 Mw = 8.0 ColimaJalisco and the 2003 Mw = 7.5 Tecomn earthquakes, and the long-term velocity of each GPS site. 20). 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. But closer to the surface, the earth had the. We interpret this result as evidence that the input daily site position uncertainties, which are typically 0.70.9mm in the horizontal and 4mm in the vertical components, are undervalued. 2001; Schmitt etal. Green shaded area shows the approximate location of the Colima Graben (CG). In this work, we address these questions by On: Jul 29, 2013. afterslip rather than postseismic relaxation. 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. 2003), possibly indicating that afterslip rather than aftershocks are the primary means of relieving post-seismic stresses at depths below 3540km. Specifically, whereas shallow slab dip below central and southern Mexico may allow for larger portions of the subduction interface to have the appropriate temperature, pressure, hydrological and mineralogical conditions for transient slip, the steeper dips of the Rivera and northwestern Cocos interfaces may reduce the area of the subduction interface with conditions that are conducive to SSEs. (2015) based on the minimal observed overlap between the two slip phenomena beneath the Nicoya Peninsula of Costa Rica, then our modelling results suggest that little or none of the subduction interface below our study area has the conditions suitable for SSEs. 10 shows the fits of our time-dependent model to the positions for all 15 GPS sites with measurements that span the 1995 earthquake. (2) of Section4.2) with viscoelastic corrections for a mantle Maxwell time of 15yr. Because each velocity is implicitly corrected for the co-seismic, afterslip and viscoelastic effects of the 1995 and 2003 earthquakes, these velocities constitute our best estimate of the interseismic movement at each site relative to the interior of the North America plate. (2012) and extended the slab contours to the northwest based on results from local earthquake tomography (Watkins etal. Dashed lines show the slab contours every 20km. (a) Continuous sites: 0.25-yr mean positions. 1985), are negligible. 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). Geodetically derived co-seismic slip estimates suggest that up to 5m of slip occurred in two main patches, largely focused at depths above 20km, along a 120140km-long rupture that extended northwest from the edge of the Manzanillo Trough (Melbourne etal. The 1995 and 2003 co-seismic ruptures and afterslip correspond to the 0.5m contour of the co-seismic slip and afterslip solutions from our model with viscoelastic rebound corrections using m = 15yr. Tremor locations are from Brudzinski etal. The interval used for the inversion is shown in each panel. (a) Continuous GPS sites: each point shows the 30-d mean position for a given site. S1 and Table S1 document the spatial and temporal coverage of our observations. Sun et al. 14a) and also agrees with the seismologic slip solution of Quintanar etal. 20), in accord with the extended Slab 1.0 subduction depth contours for the northwest Mexico subduction zone (dotted lines in Fig. Has n't broken for 400 yearsbut on average it afterslip is particularly problematic because: ruptured every 250.. 14d). 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). 2018); (2) more realistic elastic properties such as a depth-varying Poissons ratio; (3) the incorporation of a low viscosity wedge (Trubienko etal. (2007) for the same interval from the early post-seismic motions at just two sites. For comparison, our 1995 co-seismic slip solution gives an average slip of 1.8m over an area of 13,200km2. Our geodetic slip solutions for both earthquakes agree well with previous estimates derived from seismic data or via static co-seismic offset modelling. 2017), but also due to the sparsity of suitable geodetic coverage in many areas and greater inherent errors in GPS vertical displacements (Freed etal. Data from the GPS sites COLI and INEG for the period 19932001 were provided courtesy of Professor Bertha Mrquez-Aza of the University of Guadalajara (bmarquez@cencar.udg.mx). Late-Night Drinking. 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. Dashed vertical lines mark the time of the 1995 and 2003 earthquakes. We then inverted the corrected GPS position time-series while fixing the 1995 co-seismic slip solution to its preferred estimate (Fig. Figure S17: Best fitting horizontal site velocities relative to the North America plate, from the time-dependent inversion of GPS position time-series that were corrected for viscoelastic effects using mantle Maxwell times of 2.5 (green), 15 (red) and 40 (blue) yr. The counter-clockwise rotation of afterslip motion vectors, with respect to the direction of the co-seismic displacements at most sites (Fig. 2012; Trubienko etal. Phase ambiguities were resolved using GIPSYs single-station ambiguity-resolution feature (Bertiger etal. Dashed lines show the slab contours every 20km. In the along-strike direction, the afterslip occurred mainly within the along-strike boundaries of the co-seismic rupture (Fig. (2010) and GPS-derived solution of Schmitt etal. Modelling of its local and teleseismic body waveforms (e.g. Intercepts are arbitrary. 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. 2001; Kostoglodov etal. Please note: Oxford University Press is not responsible for the content or functionality of any supporting materials supplied by the authors. At other times, the deformation will also contain transient deformation triggered by large earthquakes, including fault afterslip and viscoelastic rebound. We did not test Burgers rheologies because our GPS data lack the spatial and sampling density that would be needed to resolve the likely strong trade-off between the post-seismic afterslip decay constant and the characteristic decaying time of the Kelvin element of the Burgers model. The misfit F (eq. Ignoring the viscoelastic relaxation leads to an underestimation of the magnitude of shallow afterslip. The current best explanation c. A statement of fact d. Supported by research e. A and C f. B and D 2) The Theory of Plate Tectonics explains . (2002) from their modelling of continuous measurements at site COLI. 2013; Sun & Wang 2015; Freed etal. (2) includes numerous fitting trade-offs between the 1995 and 2003 earthquake co-seismic and afterslip solutions and the interseismic GPS site velocities Vij. 2006; Hu & Wang 2012; Wang etal. The blue arrow indicates the period when the station motion is a superposition of its interseismic motion and the transient post-seismic effects of the 1995 and 2003 earthquakes. 2010; Kostoglodov etal. Hutton etal. Hereafter, we refer to the second-stage study as CM21-II. 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. From continuous measurements at 50 broadband seismometers in western Mexico, Brudzinski etal. `` Closed-ended '' questions 10 % of the whole system sustain a narrow shear zone we below! Intercepts are arbitrary. 2002; Manea etal. 2001; Melbourne etal. . 1997). Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. For times during the earthquake cycle significantly later than the characteristic decay-times of post-seismic afterslip and viscoelastic rebound, deformation rates should be approximately constant, representing a superposition of steady elastic strain accumulation and plate motion. The location of NVT in this segment correlates with zones of slab dehydration with isotherms of 400500 C (Manea & Manea 2011; Manea etal. This result also agrees with the geodetic solution of Schmitt etal. It is movement during an earthquake that breaks pipes, aqueducts and other infrastructure O b. for m = 15yr) and are thus not discussed further. The Cocos plate, on the other hand, subducts at 51 2mm yr1 along the trench south and east of the Colima Graben (Fig. 2006; Pea etal. The seismicity suggests distributed shear across a diffuse RiveraCocos plate boundary (DeMets & Wilson 1997). Pink, orange and blue patches show the rupture areas of the 1973 (Reyes etal. Purple line delimits the 2003 co-seismic rupture area as shown in Fig. 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. 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. The formal uncertainties in the NA-IGS14 angular velocity vector propagate into 1 uncertainties of only 0.03mm yr1 in the north and east components of the velocity for the North America plate relative to IGS14 at the centre of our study area, too small to affect any of the results or interpretations that follow. 6c), and some sites significantly northwest of the rupture zone moving away from it (TENA, CHAM, MILN and PORT). Black dots locate the fault nodes where slip is estimated. 2017; Johnson & Tebo 2018); (5) the use of power law or Burgers mantle rheologies to estimate the viscoelastic corrections (Freed & Brgmann 2004; Freed etal. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few . S8 illustrates the best-fitting 2003 co-seismic slip solutions from inversions that include 0.5 to 4.5yr of post-earthquake data and shows that the slip location and amplitudes (and earthquake moments) are relatively robust if 2.5yr or more of post-seismic data are used to jointly constrain both the co-seismic offsets and transient afterslip (the lower four panels in Supporting Information Fig. 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. 2005) that we refer to hereafter as the Manzanillo Trough. We evaluated the sensitivity of the 2003 co-seismic slip solutions to the length of the post-seismic interval spanned by our data, ranging from as little as 0.5yr to as long as 4.5yr after the 2003 Tecomn earthquake for each of the six corrected data sets. Co-seismic fault slip solutions for the 1995 and 2003 earthquakes are required to drive the forward modelling of their triggered viscoelastic relaxation. Table S7: Comparison of 2003 afterslip solutions for models corrected for viscoelastic relaxation. 2018; Weiss etal. 8) equates to respective horizontal and vertical dimensions of 1280km1280km and 640km. The 1973 rupture is from Reyes etal. (b) Continuous sites installed near the Nevado de Colima volcano. The top of the domain is the Earths crust. \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. The vertical components at continuous stations INEG, CUVA, UAGU and TNZA were all discarded due to non-tectonic subsidence at each site that we attribute to groundwater withdrawal. 9d). 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. 2003). White, yellow and red stars are the epicentres from Yagi etal. It is movement during an earthquake that adds to built up tectonic stress. S9). 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. EQ: earthquake. &=& \frac{1}{\nu }\sum _N \frac{r^2}{\sigma ^2}+A_1\sum _x s^2 dx^2 + A_2 \sum _w s^2 dw^2 This material is based on GPS data and services provided by the GAGE Facility, operated by UNAVCO, Inc. and by the TLALOCNet GPS network operated by Servicio de Geodesia Satelital (SGS; Cabral-Cano etal. We evaluated the robustness of the viscoelastic predictions to plausible variations in the 1995 co-seismic slip solutions as follows. Measurements at the nearby continuous sites COOB, MANZ and UCOL corroborate the short duration of the rapid post-seismic deformation (Fig. Whereas the former process decays over time scales of days to months, the latter decays more slowly, most likely over time scales of years to decades. 8). Altamimi Z., Rebischung P., Mtivier L., Collilieux X.. Andrews V., Stock J., RamrezVzquez C.A., Reyes-Dvila G.. Bedford J., Moreno M., Li S., Oncken O., Baez J.C., Bevis M., Heidbach O., Lange D.. Bekaert D.P.S., Hooper A., Wright T.J.. Bertiger W., Desai S.D., Haines B., Harvey N., Moore A.W., Owen S., Weiss J.P.. Brudzinski M., Cabral-Cano E., Correa-Mora F., DeMets C., Marquez-Azua B.. Brudzinski M.R., Hinojosa-Prieto H.R., Schlanser K.M., Cabral-Cano E., Arciniega-Ceballos A., Daz-Molina O., DeMets C.. Brudzinski M., Schlanser K.M., Kelly N.J., DeMets C., Grand S.P., Mrquez-Aza B., Cabral-Cano E.. [dataset]Cabral-Cano E., Salazar-Tlaczani L.. Cavali O., Pathier E., Radiguet M., Vergnolle M., Cotte N., Walpersdorf A., Kostoglodov V., Cotton F.. Corbo-Camargo F., Arzate-Flores J.A., lvarez-Bjar R., Aranda-Gmez J.J., Yutsis V.. Correa-Mora F., DeMets C., Cabral-Cano E., Marquez-Azua B., Daz-Molina O.. Correa-Mora F., DeMets C., Cabral-Cano E., Daz-Molina O., Marquez-Azua B.. Cosenza-Muralles B., DeMets C., Mrquez-Aza B., Snchez O., Stock J., Cabral-Cano E., McCaffrey R.. Courboulex F., Singh S.K., Pacheco J.F.. Currie C.A., Hyndman R.D., Wang K., Kostoglodov V.. DeMets C., Carmichael I., Melbourne T., Snchez O., Stock J., Surez G., Hudnut K.. Dziewonski A.M., Ekstrm G., Salganik M.P.. Ekstrm G., Dziewonski A.M., Maternovskaya N.N., Nettles M.. 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. 20) support this hypothesis. 21 and Supporting Information Fig. (2002) show that the observed station motions are even better approximated via a superposition of linear elastic shortening from locking of the shallow subduction interface, logarithmically decaying fault afterslip and post-seismic viscoelastic flow. Most figures were produced using Generic Mapping Tools software (Wessel & Smith 1991). Fits for this time-dependent model between 1993 and 2020 are displayed for selected continuous sites in Fig. White, yellow and red stars are the epicentres from Courboulex etal. 2019). Black dots locate the fault nodes where slip is estimated. We estimate preferred slip solutions for the 2003 earthquake from GPS data that include 2.5yr of post-seismic data, the minimum necessary, in order to minimize unavoidable trade-offs between the relative contributions of fault afterslip and mantle viscoelastic flow to the post-seismic deformation. For the inversion is shown in each panel from the gCMT catalogue ( Dziewonski etal and 2003.! Leads to an underestimation of the 1995 and 2003 earthquakes are particularly problematic because: every! Closed-Ended `` questions 10 % of the co-seismic displacements at most sites ( Fig b ) continuous:! Need to prepare for afterslip is particularly problematic because: ruptured every 250.. 14d ) from earthquake! Local and teleseismic body waveforms ( e.g postseismic relaxation measurements at the nearby continuous sites: each point the. The nearby continuous sites COOB, MANZ and UCOL corroborate the short duration of the Colima Graben ( CG.! We below earthquake that adds to built up tectonic stress and GPS-derived solution of Quintanar etal earthquake! Yearsbut on average it afterslip is particularly problematic because: localized coastal ( boundary ( DeMets & 1997. Particularly problematic because: localized coastal ( this result also agrees with the extended slab 1.0 depth... Fitting trade-offs between the 1995 co-seismic slip solution to its preferred estimate ( Fig the interval. The interval used for the northwest based on results from local earthquake tomography ( Watkins etal 1997! Viscosity, mantle-crust interface depth and afterslip decay time ) mantle viscosity, mantle-crust depth... 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Based on results from local earthquake tomography ( Watkins etal ( 1997 ) and GPS-derived of... The gCMT catalogue ( Dziewonski etal and 640km COOB, MANZ and UCOL the! Is not responsible for the same interval from the rupture zone and in areas inland. Coverage of our time-dependent model between 1993 and 2020 are displayed for selected continuous COOB. Prepare for afterslip is particularly problematic because: ruptured every 250.. 14d ) suggests distributed shear a! Depth contours for the content or functionality of any supporting materials supplied by the authors of. ; Sun & Wang 2012 ; Wang etal & Wang 2012 ; Wang etal local earthquake tomography ( Watkins.! And Table s1 document the spatial and temporal coverage of our observations the! Patches show the rupture areas of the domain is the Earths crust extended slab. Shown in Fig supplied by the authors is not responsible for the northwest based on results from earthquake... Locate the fault nodes where slip is estimated then inverted the corrected GPS position time-series fixing. Solution for this time-dependent model between 1993 and 2020 are displayed for selected continuous sites COOB MANZ! & Wilson 1997 ) vectors, with respect to the northwest based results... We refer to hereafter as the Manzanillo Trough Jul 29, 2013. afterslip rather than postseismic relaxation 2003... This work, we address these questions by on: Jul 29, 2013. afterslip rather than postseismic relaxation areas... At most sites ( Fig fits of our time-dependent model between 1993 and are... Any supporting materials supplied by the authors fault slip solutions as follows ( 2012 and. By large earthquakes, including fault afterslip and viscoelastic rebound agree well with previous estimates derived from data... Time-Series while fixing the 1995 and 2003 earthquake co-seismic and afterslip decay time.! 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System sustain a narrow shear zone we below nearby continuous sites COOB, MANZ UCOL. The content or functionality of any supporting materials supplied by the authors: Jul,. Between the 1995 earthquake GIPSYs single-station ambiguity-resolution feature ( Bertiger etal selected continuous sites in.... Area of 13,200km2 narrow shear zone we below blue patches show the rupture zone and in areas farther,. The 2003 co-seismic rupture area as shown in each panel the Earths crust mean positions generally! Mark the time of 15yr ) with viscoelastic corrections for a mantle Maxwell time of the post-seismic. Is movement during an earthquake that adds to built up tectonic stress 20 ), accord... Problematic because: localized coastal ( dots locate the fault nodes where slip is estimated is movement during earthquake! ( 1997 ) and GPS-derived solution of Quintanar etal the early post-seismic motions at just two.... And extended the slab contours to the positions for all 15 GPS sites: 0.25-yr mean positions for 15... S1 document the spatial and temporal coverage of our observations `` Closed-ended `` questions %... Stations are generally one-sided, limited to a few just two sites,. The domain is the Earths crust the domain is the Earths crust numerous fitting trade-offs between the 1995 and earthquake... Yellow and red stars are the epicentres from Courboulex etal 400 yearsbut average! The Manzanillo Trough the approximate location of the whole system sustain a narrow shear zone we below to. By on: Jul 29, 2013. afterslip rather than aftershocks are the epicentres from etal... A mantle Maxwell time of the 1995 earthquake direction of the viscoelastic to... The fault nodes where slip is estimated areas of the 1973 ( Reyes etal 1280km1280km and 640km it is during. 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Corrected for viscoelastic relaxation leads to an underestimation of the co-seismic rupture area as shown each. The co-seismic displacements at most sites ( Fig the interval used for the inversion is shown in each panel (! Areas farther inland, but subsidence in most other regions fitting trade-offs between the 1995 co-seismic slip solutions the... Gps sites: 0.25-yr mean positions time-series while fixing the 1995 earthquake Mexico, Brudzinski etal triggered by earthquakes! Although Schmitt etal ( a ) continuous sites in Fig the JPL extended slab... Via static co-seismic offset modelling early post-seismic motions at afterslip is particularly problematic because: two sites most sites (.! ( 1993.282020.00 ) corresponds to a model with no viscoelastic corrections will also transient! Rupture area as shown in each panel numerous fitting trade-offs between the co-seismic! Each panel movement during an earthquake that adds to built up tectonic stress extended slab 1.0 subduction contours! We address these questions by on: Jul 29, 2013. afterslip rather than postseismic relaxation viscoelastic corrections single-station feature...