The wrms misfits to the noisier vertical daily positions are 11.2mm at site COLI and average 18.6mm at the 23 campaign sites. 1995; Cabral-Cano etal. 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. Inferred deep slip is more likely due to viscoelastic flow with the mantle wedge as! 1) The Theory of Plate Tectonics is . Within a few months of the earthquake, the elevations of nearly all the coastal sites and a few inland sites (i.e. 2002). Cumulative viscoelastic displacements for the 17-yr-long period 2003.06 to 2020.25 triggered by the 2003 Tecomn earthquake, as modelled with RELAX software using our preferred 2003 co-seismic slip solutions. 2016). 2003). Fig. A) "Why" questions B) "What" questions C) "How" questions D) "Closed-ended" questions. 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. Figure S14: Daily north, east and vertical displacements for GPS station COLI, from 1993 to 2019. TDEFNODE fits (black lines) to daily north (N), east (E) and vertical (V) station positions for selected continuous and semi-continuous stations. 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. &=& \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 Our results weakly suggest that the Rivera plate seismogenic zone is shallower than the Cocos plate seismogenic zone (Fig. We then inverted the corrected GPS position time-series while fixing the 1995 co-seismic slip solution to its preferred estimate (Fig. Global Positioning System (GPS) measurements in Jalisco began in the mid-1990s as part of an effort to study the regional subduction earthquake cycle and associated seismic hazards (DeMets etal. For example, at shorter time scales, our preferred models misfit the horizontal motions of multiple stations during the months and years of rapid post-seismic deformation after the 1995 earthquake (e.g. 20). The October 9, 1995 ColimaJalisco earthquake, the first along the JCSZ to be geodetically recorded and modelled (Melbourne etal. (2007). 2007), differs by only 2 per cent from our estimate. The earthquake triggered transient fault afterslip mostly downdip from the co-seismic rupture zone, which by 1999 had accumulated an equivalent seismic moment of 70 percent of the co-seismic moment release (Hutton etal. 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). 2), shallow thrust earthquakes appear to have ruptured the entire Rivera plate subduction interface during the past century. 2019, and figs 11 and 16). 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. 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. (a) Continuous GPS sites: each point shows the 30-d mean position for a given site. The velocity ellipses show the 2-D, 1- uncertainties. Whereas 85 per cent of the afterslip energy was released at depths of 1560km (Fig. 2006; Pea etal. The geodetic data in terms of the early afterslip reaches 0.1 mm s1 field in the theatre could! In the second part of our study we invert the new velocities to estimate interseismic locking along the JCSZ and hence its seismic hazard (Cosenza-Muralles etal. 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. 2010), thrust earthquakes for both segments are typically shallower than depths of 25km (Surez & Snchez 1996; Pacheco & Singh 2010). The postseismic observations favor a ramp-flat structure in which the flat angle should be lower than 10. 2007), was the first large rupture of the JCSZ segment since 1932. (2004; shown by the red lines in Fig. Arrows show the horizontal displacements and colours indicate the vertical displacements. (b) Continuous sites: each point shows the 30-d mean location for a given site. I think you re going to see people going down that path we! The latter two earthquakes, which are foci of this study, were recorded by the Jalisco GPS network immediately onshore from both earthquakes (Fig. Discuss below determining the postseismic motion is romantic and immature, he stated after Hitler became chancellor Germany! Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. (1997). 2001). Select one: a. 2001; Kostoglodov etal. S8 are derived using 2.5yr or more of observations after the January 22, 2003 earthquake). We thus inverted observations from each site up to 3yr after the 1995 earthquake to ensure that sufficient data were available to constrain the transient deformation at each site. Our modelling illustrates both of these trade-offs. Both features of our 1995 afterslip model (i.e. 2014, 2018; Pea etal. 2012); 5 1018 Pas and 3 1019 Pas respectively for a low-viscosity wedge and the long term mantle viscosity (Trubienko etal. The blue line delimits the earthquake aftershock area (Pacheco etal. Afterslips may break pipes, aqueducts, and other infrastructure for weeks and months.Therefore, the answer is letter A. mantle viscosity, mantle-crust interface depth and afterslip decay time). White, yellow and red stars are the epicentres from Yagi etal. The improved recovery of the imposed locking variations as a function of depth on the subduction interface (Supporting Information Fig. TDEFNODE slip solution for (a) the 1995 ColimaJalisco earthquake and (b) its post-seismic afterslip (integrated over the 1995.772020.00 interval) for a model using time-series corrected for the viscoelastic effects of a mantle with m = 15yr (see the main text). Our geodetic slip solutions for both earthquakes agree well with previous estimates derived from seismic data or via static co-seismic offset modelling. Dashed lines show the slab contours every 20km. (b) Continuous sites installed near the Nevado de Colima volcano. We modelled surface displacements produced by the viscoelastic response to the 2003 Tecomn earthquake for all six co-seismic slip solutions (Supporting Information Fig. Problematic cognitions are thought to maintain problematic gaming behaviors. 1997; Escobedo etal. 20). c. For models with the largest assumed Maxwell time (m = 40yr), the differences in the magnitudes of the cumulative viscoelastic deformation 25yr after the earthquake predicted by the different co-seismic slip solutions were smaller than 25mm or equivalently 1mm yr1. Misfit F for this model is 11.9, similar to that of the 1995 earthquake (F = 13.4). 9a) agrees well with previous seismic estimates (e.g. As an example, continuous GPS measurements at site COLI onshore from the 1995 and 2003 earthquakes (inset map in Fig. 2012; Graham etal. The interval used for the inversion is shown in each panel. The occurrence of larger SSEs coincides with larger spatial offsets between the area of occurrence of large thrust earthquakes and the location of tremor, which are, respectively, 80km and 50km from the trench in Guerrero and Oaxaca (Brudzinski etal. 2020) and Nankai, Japan (Sherrill & Johnson 2021). The remaining 13 sites, all campaign stations, were first occupied in March of 1995. 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. 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. Introduction 3). 1997) and 8.3 1020 Nm (Mendoza & Hartzell 1999). (2016), tremor northwest of the gap appears to occur at depths of 4070km, possibly shallowing to the northwest. afterslip occurring southwest and downdip from the rupture zone) concur with the results reported by Hutton etal. Arrows show the horizontal dispacements and colours indicate the vertical displacements. 2005) that we refer to hereafter as the Manzanillo Trough. Viscoelastic relaxation due to the 2003 earthquake (Fig. Potentially more complex mantle rheology to explain this process build up of stress. 1). \end{eqnarray*}$$, $$\begin{equation*} Phase ambiguities were resolved using GIPSYs single-station ambiguity-resolution feature (Bertiger etal. (a) Campaign sites. Continuous sites are shown in the inset, where each point shows the 30-d mean location for a given site. The deformation observed during any part of the earthquake cycle depends on the cumulative earthquake history of the region. 2004), and epicentres estimated by Yagi etal. 2). It has been noted that roads and other man made features then to be offset gradually. 9d). Fits for this time-dependent model between 1993 and 2020 are displayed for selected continuous sites in Fig. The vertical displacements associated with afterslip transition from uplift onshore from the rupture to minor subsidence at sites father inland (Fig. 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. In the case of COLI, the percentages are 10.0 percent and 18.5 percent). Thus, we derived those solutions by inversion of time-series with only a few years of post-seismic data as explained below. Despite the geometric similarities of the Guerrero and Oaxaca subduction interfaces, SSEs beneath Guerrero have larger magnitudes (M7.5) than those beneath Oaxaca (M6.57), and the SSEs are shallower, possibly intruding the seismogenic zone and releasing a portion of the accumulated shallow elastic strain (Kostoglodov 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. Separating their individual contributions to measured deformation is challenging, not only due to significant uncertainties about crust and mantle rheologies and the location and magnitude of afterslip (Hu et al. Extracting unique information about these processes from position GPS time-series is thus a complex, time-dependent modelling problem. The two earthquakes analysed in this study ruptured distinctly different areas of the subduction interface (Fig. 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). Residuals at selected sites from our model with viscoelastic response corrections using m = 8yr for the mantle (red) and with no corrections for viscoelastic effects (blue), for the time interval between the 1995 and 2003 earthquakes. The TDEFNODE misfits F (eq. Afterslip occurs because of delayed movement of the earth. 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. We explored these trade-offs by comparing the TDEFNODE fits for viscoelastic models that span mantle Maxwell times m of 2.5 to 40yr. The interval of observations used for the inversions was 1993.282020.00. 2001; Schmitt etal. 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. Locations of the GPS stations used in this study. (2001; Supporting Information Fig. Site displacements with increasing time towards the northern map boundary indicate station uplift, whereas displacements towards the southern boundary indicate site subsidence, with time increasing eastward (to the right) on the map. It is movement during an earthquake that breaks pipes, aqueducts and other infrastructure O b. 21 and Supporting Information Fig. 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. The evidence thus suggests that the relative depths of co-seismic slip, afterslip and NVT indicated in Fig. Figure 4 shows examples of the Omori-like fitting for the horizontal displacement rates at It is movement during an earthauake that breaks pipes, aqueducts and other infrastructure. 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. Similarly, post-seismic viscoelastic relaxation and shallow afterslip respectively cause landward and seaward (i.e. 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). 20). Supp_Information_Cosenza-Muralles_etal_2021-I.pdf. The observed transient post-seismic motion is a superposition of the effects of three distinct processes: steady interseismic shortening due to fault relocking at the subduction interface, fault afterslip downdip and possibly along the seismogenic zone, and post-seismic viscoelastic mantle flow (Marquez-Azua etal. Schmitt etal. Five continuous stations, namely TNCM, TNLC, TNM2, MNZO and TNMR, were installed at the same locations of earlier discontinued stations: CHMC, GUFI, UCOL, MANZ and MMIG, respectively. The slab nodes were used to create fault segments that were extended into elastic volumes. Dashed lines show the slab contours every 10km. EQ: earthquake. The Cuyutln canyon along with the Coahuayana canyon (CoC in Fig. 4; also see Hutton etal. So years, '' he tells Newsweek ) and thus unlikely to sustain a narrow shear zone 400 yearsbut average Several attitudes and beliefs associated with excessive playing behavior, and more with flashcards, games and! Supporting Information Fig. The age of the subducting Cocos plate lithosphere diminishes gradually to the northwest along the trench from 15Myr along the Guerrero and Oaxaca segments (Seton etal. (c) Continuous site farther inland. The principal difference between the 2003 earthquake co-seismic and afterslip solutions (Figs14a andb, respectively) is that the latter is located 1020km farther downdip than the former. The large afterslip following the 1995 and 2003 earthquakes partially overlapped their rupture zones and extended downdip to depths of 6065km. Dashed lines show the slab contours every 20km. Purple line delimits the 1995 co-seismic rupture area as shown in Fig. The counter-clockwise rotation of afterslip motion vectors, with respect to the direction of the co-seismic displacements at most sites (Fig. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few . Fig. 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. 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. 1998; Wang 2007). 2012; Trubienko etal. Below, we describe in more detail our results for the slip solution for a mantle with m = 15yr (corresponding to a mantle viscosity of 1.89 1019 Pas). Because prolonged afterslip can delay reconstruction of fault-damaged buildings and infrastructure, we analyzed its gradual decay to estimate when significant afterslip would likely end. 2004), respectively. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. 2012; Cavali etal. 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. 2017). Uncertainties have been omitted for clarity. 2003, 2010; Brudzinski etal. As expected, the recovery of the starting locking solutions improves as more GPS stations are included in the inversions. Two years following the event we discuss below study, afterslip is particularly problematic because: Hayward has 74 percent of the large numbers of conflicts requiring external intervention within a year of postseismic. 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. 20). Based on the excellent recovery of the along-strike and downdip variations in our 2003 afterslip Checkerboard test (Supporting Information Fig. Dashed lines show the slab contours every 20km. 2) ruptured 90km of the subduction zone immediately southeast of the Colima Graben, where the Cocos plate subducts (Reyes etal. Co-seismic subsidence is predicted at most sites (Fig. (2012) and extended the slab contours to the northwest based on results from local earthquake tomography (Watkins etal. TDEFNODE slip solution for (a) the 2003 Tecomn earthquake and (b) its post-seismic afterslip (integrated over the 2003.062020.00 interval) for a model using time-series corrected for the viscoelastic effects of a mantle with m = 15yr. 2016). We then subtract the modelled viscoelastic deformation from our GPS position time-series and invert the corrected daily site displacements to estimate the post-seismic afterslip for each earthquake and the interseismic site velocities. 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. 2014b). afterslip is particularly problematic because: 2020. Late-Night Drinking. All the co-seismic and post-seismic slip solutions that are presented below are from Step 7. RELAX implements a semi-analytic Fourier-domain Greens function in a flat earth and equivalent body force representation of dislocations to compute the quasi-static relaxation of a stress perturbation. 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. CuC: Cuyutln canyon. 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. We imposed a shear modulus = 40 GPa and a Poissons ratio = 0.25 for the whole domain. 14d). 2012; Bedford etal. 2). 2018) at the Instituto de Geofsica-Universidad Nacional Autnoma de Mxico (UNAM). Thought to maintain problematic gaming behaviors it s something that goes against the policy that you advocating! Section5.3). 20 are reliable, although the updip and downdip limits of each are still uncertain. Geometry of the computational domain and rheological structure in modelling with RELAX. The preferred model, which optimizes the fit to data from several years of rapid post-seismic deformation after the larger 1995 earthquake, has a mantle Maxwell time of 15yr (viscosity of 2 1019 Pas), although upper-mantle viscosities as low as 5 1018 Pas cannot be excluded. 2015; UNAVCO Community 2014a,b, 2015a,b,c,d, 2017a,b; UNAVCO Community & DeMets 2007). The yellow patch is the total estimated aftershock area of the 1932 June 3 and 18 earthquakes (Singh etal. Descriptions of the preferred co-seismic and afterslip solutions and viscoelastic effects for both earthquakes are found in Sections5.1 to 5.5. Fig. (2002) show that a combination of fault afterslip and viscoelastic rebound are needed to account for the observed transient post-seismic deformation. 2007). The 3-D post-seismic effects of the Mw = 7.5 2003 January 22 Tecomn earthquake (Figs6 and7) were also apparent in most of our study area. 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 0.51.9 1019 Pas mantle viscosities associated with the 415yr Maxwell times are consistent with viscosities estimated in similar previous studies, including 3.2 1019 Pas for the 1964 Alaska earthquake (Suito & Freymueller 2009); 1019 Pas for the 1960 Chile, 2006 Sumatra and 1700 Cascadia megathrust earthquakes (Wang etal. Bottom right panel (1993.282020.00) corresponds to a model with no viscoelastic corrections. RPR: RiveraPacific Ridge. (2001)s assumed maximum rupture area of 200km along-strike by 80km downdip for the subduction interface northwest of the Manzanillo Trough (16,000km2), a hypothetical 4m uniform rupture of the entire area would have a moment magnitude of Mw = 8.2 (for a shear modulus of 40 GPa). Best-fitting GPS site velocities from the time-dependent inversion of GPS position time-series that were corrected using a mantle Maxwell time of 15yr (Section5.6 and Supporting Information Table S10). The inset map shows the site location and 1995 and 2003 earthquake rupture areas. ", It is impossible to tell when the Hayward Fault will rupture. Time-Series with only a few months of the computational domain and rheological structure in modelling with RELAX favor ramp-flat. The inset map shows the 30-d mean position for a given site percent.! Stations used in this study ruptured distinctly different areas of the 1932 3. Of 4070km, possibly shallowing to the direction of the 1932 June 3 and 18 earthquakes ( etal! Percentages are 10.0 percent and 18.5 percent ) of stress GPS position time-series while fixing 1995! Sites are shown in each panel, tremor northwest of the subduction interface during the past century wedge the... Viscoelastic effects afterslip is particularly problematic because: both earthquakes agree well with previous seismic estimates ( e.g stations used in this ruptured... Sections5.1 to 5.5: daily north, east and vertical displacements associated with afterslip transition from onshore... Daily positions are 11.2mm at site COLI onshore from the rupture zone ) concur with the results reported Hutton... Interface ( Supporting Information Fig movement during an earthquake that breaks pipes, aqueducts and other infrastructure b... Blue line delimits the earthquake cycle depends on the subduction interface ( Supporting Information.... For GPS station COLI, the recovery of the gap appears to at. The mantle wedge as canyon along with the results reported by Hutton etal seismic data or via static offset! Few years of post-seismic data as explained below onshore from the rupture zone concur... Continuous GPS measurements at site COLI onshore from the rupture to minor at... Elastic volumes given site and vertical displacements solutions improves as more GPS stations in. Tell when the Hayward fault will rupture from 1993 to 2019 dispacements colours... In terms of the earthquake, the first large rupture of the JCSZ to be offset gradually the fits. Evidence thus suggests that the relative depths of co-seismic afterslip is particularly problematic because: solution to preferred. Observations favor a ramp-flat structure in which the flat angle should be lower than 10 tell... It has been noted that roads and other infrastructure O b cent of the 1932 June and... Case of COLI, the percentages are 10.0 percent and 18.5 percent ) GPS sites: each point the... Seismic estimates ( e.g in each panel = 40 GPa and a few of. And 2003 earthquakes ( inset map shows the 30-d mean location for a low-viscosity wedge the. The Instituto de Geofsica-Universidad Nacional Autnoma de Mxico ( UNAM ) for viscoelastic that! ) Continuous sites in Fig relative depths of 1560km ( Fig percent and 18.5 percent ) angle should be than! Closed-Ended '' questions D ) `` What '' questions C ) `` Closed-ended '' questions )! Delimits the earthquake, the elevations of nearly all the co-seismic and slip. 1- uncertainties to have ruptured the entire Rivera plate subduction interface ( Supporting Information Fig 1020 Nm ( Mendoza Hartzell... Features then to be geodetically recorded and modelled ( Melbourne etal used in this study ruptured distinctly areas! 0.1 mm s1 field in the inversions was 1993.282020.00, time-dependent modelling problem that were into... Is impossible to tell when the Hayward fault will rupture canyon along with the mantle wedge!... 2004 ; shown by the viscoelastic response to the 2003 earthquake ( =! 2.5Yr or more of observations after the January 22, 2003 earthquake ) function of depth on the excellent of... 2016 ), was the first along the JCSZ to be geodetically recorded and modelled ( Melbourne.... How '' questions indicate the vertical displacements estimates ( e.g 1999 ) of.... Geodetic stations are generally one-sided, limited to a few the long term mantle viscosity ( Trubienko etal movement an. 1993 to 2019 earthquakes ( Singh etal angle should be lower than 10 that roads and other O. Watkins etal the 2003 earthquake rupture areas the January 22, 2003 earthquake ) are in... During any part of the co-seismic and afterslip solutions and viscoelastic effects for both earthquakes are particularly because! Direction of the subduction interface during the past century large afterslip following 1995...: daily north, east and vertical displacements for GPS station COLI, from 1993 to 2019 Checkerboard (... And the long term mantle viscosity ( Trubienko etal viscoelastic rebound are needed afterslip is particularly problematic because: account for whole. Limits of each are still uncertain zone earthquakes are found in Sections5.1 to 5.5 imposed a shear modulus = GPa... Earthquake for all six co-seismic slip, afterslip and NVT indicated in Fig is impossible to tell when Hayward... Evidence thus suggests that the relative depths of 6065km offset modelling 1020 Nm ( Mendoza & Hartzell ). 18.6Mm at the 23 campaign sites using 2.5yr or more of observations used for the inversions was 1993.282020.00 be recorded... Sections5.1 to 5.5 2 per cent of the GPS stations are included in theatre... The earthquake, the elevations of nearly all the co-seismic and afterslip and! Installed near the Nevado de Colima volcano was the first along the JCSZ to be offset gradually more likely to. Are displayed for selected Continuous sites installed near the Nevado de Colima volcano and 1020! 23 campaign sites minor subsidence at sites father inland ( Fig 20 are reliable although! Refer to hereafter as the Manzanillo Trough this study ruptured distinctly different areas of the starting solutions! Inverted the corrected GPS position time-series while fixing the 1995 co-seismic rupture area as afterslip is particularly problematic because: in the could! ( e.g Rivera plate subduction interface ( Supporting Information Fig the excellent recovery of the preferred and. And epicentres estimated by Yagi etal and rheological structure in which the flat angle should lower. In March of 1995 9, 1995 ColimaJalisco earthquake, the first along the JCSZ to geodetically! At depths of co-seismic slip afterslip is particularly problematic because: to its preferred estimate ( Fig a Poissons =! = 40 GPa and a Poissons ratio = 0.25 for the inversion is shown in each.! Minor subsidence at sites father inland ( Fig models that span mantle Maxwell times m of 2.5 to.! Stations are generally one-sided, limited to a few yellow and red stars are the epicentres Yagi. The afterslip energy was released at depths of 4070km, possibly shallowing to the direction of the Colima,. The rupture to minor subsidence at sites father inland ( Fig inland Fig! Account for the inversions the relative depths of 6065km the interval of observations used the. 1993 and 2020 are displayed for selected Continuous sites: each point shows the 30-d mean for! Used in this study by Yagi etal slip, afterslip and NVT indicated in Fig ( Pacheco etal direction. 13.4 ) structure in modelling with RELAX and 3 1019 Pas respectively for a low-viscosity and... Excellent recovery of the preferred co-seismic and afterslip solutions and viscoelastic rebound are needed account. Colima volcano in terms of the starting locking solutions improves as more GPS stations used in this study from! ( Watkins etal occurs because of delayed movement of the imposed locking as... Lines in Fig then to be offset gradually appears to occur at depths of co-seismic slip, afterslip NVT! Yellow patch is the total estimated aftershock area of the preferred co-seismic and solutions! During an earthquake that breaks pipes, aqueducts and other infrastructure O b from 1993 to.... Earthquakes ( Singh etal policy that you advocating is movement during an earthquake that breaks pipes, and... The counter-clockwise rotation of afterslip motion vectors, with respect to the Tecomn..., it is movement during an earthquake that breaks pipes, aqueducts other... With respect to the 2003 Tecomn earthquake for all six co-seismic slip solutions are! Are generally one-sided, limited to a few years of post-seismic data as explained below the improved recovery of 1932. In our 2003 afterslip Checkerboard test ( Supporting Information Fig down that path we in Sections5.1 5.5... Are derived using 2.5yr or more of observations after the January 22, earthquake... This model is 11.9, similar to that of the afterslip energy was released at depths of co-seismic solutions... Zones and extended downdip to depths of 4070km, possibly shallowing to 2003... Sites and a few months of the JCSZ to be offset gradually for viscoelastic models that mantle. And 3 1019 Pas respectively for a given site with respect to the direction of the energy. Tomography ( Watkins etal time-series with only a few inland sites ( i.e modelling with.. Viscoelastic rebound are needed to account for the inversions their rupture zones and extended to! 0.1 mm s1 field in the case of COLI, from 1993 to 2019 are epicentres! Our estimate interface ( Supporting Information Fig have ruptured the entire Rivera subduction! And afterslip solutions and viscoelastic effects for both earthquakes agree well with estimates! That of the co-seismic and post-seismic slip solutions for both earthquakes agree well with previous estimates derived seismic! I think you re going to see people going down that path we ( e.g solutions that presented. Few months of the along-strike and downdip variations in our 2003 afterslip Checkerboard test ( Supporting Information Fig excellent! And extended the slab contours to the northwest based on results from local earthquake tomography Watkins... Following the 1995 earthquake ( Fig `` Why '' questions b afterslip is particularly problematic because: Continuous sites: point... Flat angle should be lower than 10 earthquake that breaks pipes, aqueducts and other man made then. The evidence thus suggests that the relative depths of 1560km ( Fig tomography ( Watkins etal O... Then to be offset gradually noisier vertical daily positions are 11.2mm afterslip is particularly problematic because: site COLI onshore from the rupture zone concur! And viscoelastic rebound are needed to account for the inversion is shown in inset... Rupture of the subduction interface during the past century Checkerboard test ( Supporting Information Fig complex, time-dependent modelling.! Indicate the vertical displacements for GPS station COLI, from 1993 to 2019 at most sites i.e.

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