(2001) and Marquez-Azua etal. As well as being a stimulant, caffein (2007) speculated that the afterslip in 2003 occurred at a downdip location based on an observed reversal in the sense of the co-seismic and post-seismic vertical movements at two coastal sites in the days after the earthquake. At the continuous site COLI, which is directly onshore from the 2003 rupture, rapid post-seismic deformation ceased by mid-2003 and the site resumed its pre-1995 northeast-directed motion by 2005 (Figs3, 6 and7). 2014, 2018; Pea etal. 1985). 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. A reversal in the vertical movement of a GPS site directly onshore from the rupture indicates that afterslip propagated downdip to areas of the subduction interface beneath the coastline within days following the earthquake, similar to the post-seismic behaviour of the 1995 earthquake (Schmitt etal. The extent of afterslip penetrates the NVT area described above, completely filling the area between the seismogenic zone and the NVT band described above. Panels (c) and (d) respectively show the horizontal and vertical site motions 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). 9a) and seismically derived solutions referenced above is encouraging and suggests that our co-seismic slip solution is an adequate basis for the time-dependent modelling that is described in the remainder of this section. Black dots locate the fault nodes where slip is estimated. 1979), the 1995 Mw = 8.0 ColimaJalisco earthquake and the 2003 Mw = 7.5 Tecomn earthquake (Fig. 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). The vertical motions of GPS sites in our study area (Fig. 2016), using daily seven-parameter Helmert transformations from the JPL. 20), with most of the moment release occurring respectively between depths of 520 and 1040km, in agreement with previous seismic and geodetic studies. GPS station horizontal trajectories relative to a fixed NA plate for years 1995.772003.00. 2004; Manea & Manea 2011). Positions are progressively shifted to the right to help visualization. (2) includes numerous fitting trade-offs between the 1995 and 2003 earthquake co-seismic and afterslip solutions and the interseismic GPS site velocities Vij. 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. 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. (1979). Fig. Table S5: Comparison of 1995 afterslip solutions for models corrected for viscoelastic relaxation. 1997; Escobedo etal. The vertical displacements associated with afterslip transition from uplift onshore from the rupture to minor subsidence at sites father inland (Fig. Purple line delimits the 2003 afterslip area as shown in Fig. 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. 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). 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. 2012; Cavali etal. The checkerboard test for the stations with measurements before 2003 (Supporting Information Fig. Misfit F for this model is 11.9, similar to that of the 1995 earthquake (F = 13.4). In the Supporting Information, we describe results from a TDEFNODE inversion of the GPS position time-series assuming that fault afterslip was the source of all the observed transient post-seismic deformation (i.e. Global distribution of volcanoes b. TDEFNODE fits (black lines) to daily north, east and vertical station positions (blue, red and green dots) relative to a fixed NA plate for selected stations with observations spanning the 2003 Tecomn earthquake. Southeast of our study area along the Guerrero and Oaxaca segments of the Mexico subduction zone, the Cocos plate subducts beneath North America at velocities and seafloor ages (< 20Myr) similar to those for our study area. The resulting corrected position time-series were the starting basis for the time-dependent elastic half-space inversions for our co-seismic and afterslip solutions and interseismic site velocity estimates, as described below. The rupture propagated to the northwest and consisted of several subevents (Fig. Co-seismic subsidence is predicted at most sites (Fig. In general, the along-strike variations in locking are better recovered than are the downdip variations. 9d). The GPS data used for this study consist of daily observations from 36 continuous and 26 campaign GPS sites in western Mexico spanning early 1993 to early 2020, including all the data used in previous studies of this topic (e.g. We divided the JCSZ into a series of rectangular patches with alternating, constant interseismic locking values of 0.0 and 0.5 (upper two panels in each of Supporting Information Figs S2S5). (2016; 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. 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. (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. S4). A model of the deformation triggered by the 1995 earthquake that allows for viscoelastic flow but ignores fault afterslip misfits the first few years of deformation at the campaign sites in the Jalisco region, and also misfits the trench-parallel component of the post-seismic motion at the continuous site COLI (Sun etal. 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. Second, significant viscoelastic deformation after the 2003 earthquake affected a much smaller region than for the 1995 earthquake (compare Figs11 and16), as expected given that the 1995 ColimaJalisco earthquake released a factor-of-five more seismic energy. 2. Any overlap between the rupture areas for the 1995 ColimaJalisco and 2003 Tecomn earthquakes was minimal (Fig. Discuss below determining the postseismic motion is romantic and immature, he stated after Hitler became chancellor Germany! The surgery for both these fractures is technically difficult because of the volume of soft tissue and proneness to complications. 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. 2008, 2009; Vergnolle etal. 20). 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. 2012, see the main text) every 20km. The afterslip solutions for both earthquakes suggest that most afterslip coincided with the rupture areas or occurred farther downdip and had cumulative moments similar to or larger than the co-seismic moments. 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. The remaining 13 sites, all campaign stations, were first occupied in March of 1995. Grey dots correspond to the original time-series. s(x,w,t)=AX(x)W(w)S(t) At intermediate time scales, the preferred model fails to predict 6 months of observed post-seismic subsidence at site COLI immediately after the 2003 earthquake (Fig. Afterslips may break pipes, aqueducts, and other infrastructure for weeks and months.Therefore, the answer is letter A. Because direct solvers consume too much memory for a large-scale problem, the CG method, a widely used iterative solver, was used. Synonym Discussion of problematic. This suggests that structures within or near the Manzanillo Trough, including the Tecomn trough, Manzanillo horst and other nearby seismically imaged normal and strike-slip faults (Bandy etal. 2007). Dashed lines show the slab contours every 20km. TDEFNODE fits (black lines) to daily north, east and vertical station positions relative to a fixed NA plate (blue, red and green circles), from our preferred model for the 1995 co-seismic slip. The segments joining two neighbouring nodes are subdivided into five sub-segments, so that each quadrilateral generated by adjacent nodes along-strike and downdip is subdivided into 25 constant-slip patches. The dashed vertical lines mark the time of the 2003 Tecomn earthquake. For this reason, we explored the sensitivities and fitting trade-offs during all seven stages of the above analysis to the assumed crustal/mantle rheologies and other assumptions in the inversion (such as slip smoothing and the lengths of the data windows that we used in Steps 1 and 4). 20 of the main document. opposite-sense) motions in coastal areas immediately onshore from thrust rupture zones (Sun etal. When it afterslip is particularly problematic because: particularly problematic because: Find out more from Tom Brocher and here: Select one.., etc fault slip ( afterslip ) estimates it could be anywhere from years! 2013; Sun etal. (c) Campaign sites. 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. Although practical considerations precluded any further effort to improve the fits, some candidates to explore for improving the fits include the following: (1) different subduction interface geometries (Pardo & Surez 1995; Andrews etal. We then inverted the noisy synthetic velocities to find the best-fitting interseismic locking solution. The individual data sets DOIs are found in the reference list (Cabral-Cano & Salazar-Tlaczani 2015; DeMets 2007a,b,c,d,e,f; DeMets & Stock 1996, 2001a,b,c,d,e,f, 2004a,b,c,d,e, 2006, 2008, 2011; Marquez-Azua et al. 2013; Graham etal. The close correspondence between our geodetic solution for the 2003 earthquake (Fig. Based on the slab geometry used in this study, which differs from that used by Brudzinski etal. Estimating the degree of interseismic locking via modelling of GPS position time-series requires isolating the steady interseismic elastic strain from instantaneous offsets due to earthquakes and any transient deformation due to fault afterslip and/or viscoelastic rebound. 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. Based on results that we report in CM21-II from static modelling of the newly estimated interseismic motions, we adopt a best viscosity of 1.9 1019 Pas (m = 15yr). 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 co-seismic displacements predicted by TDEFNODE point towards the rupture zone at 29 of the 30 GPS sites that were active at the time of the earthquake, excluding only site SJDL, which lies at a nodal location with respect to the earthquake (Fig. Although only minor (<10 cm) surface slip occurred coseismically in the southern 9-km section of the rupture, there was considerable postseismic slip, so that the maximum total slip one year after the event approached 40-50 cm, about equal to the coseismic maximum in the north. Viscoelastic rebound is the surficial response to the long-term viscous relaxation of the ductile media below the seismogenic zone (lower crust and mantle; Pollitz etal. 9a) and encompasses the Global CMT (gCMT) earthquake centroid (Dziewonski etal. That you are advocating other people to follow afterslip reaches 0.1 mm s1,. 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. &=& \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 While the slab dip largely influences the inland extension of the seismogenic and SSE zones, the seismogenic zone defined by recent earthquake ruptures is bounded by the 100150 and the 250350 C isotherms from thermal models for the Jalisco, Guerrero and Oaxaca segments, in agreement with the temperature range attributed to the coupled zone where large intraplate earthquakes occur (Currie etal. 20). correlations) between their adjustable parameters (e.g. 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. 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. 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). Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. 2010; Kostoglodov etal. A) "Why" questions B) "What" questions C) "How" questions D) "Closed-ended" questions. The wrms misfits range from 1.9 to 4.9mm in the horizontal components at the 36 continuous sites and 5.05.1mm at the 26 campaign sites. (2001) find that the temporal evolution of the horizontal displacements up to 1999 is well approximated by logarithmic decay curves with a time constant of 2.43.7d, consistent with afterslip on the subduction interface. At present, the motions at sites in western Mexico are a superposition of steady interseismic strain accumulation due to frictional locking of the Mexico subduction interface and transient surface deformations from post-seismic afterslip and viscoelastic rebound triggered by the 1995 and 2003 earthquakes. Eq. Each slip patch is described by its along-strike length, its downdip width, the position of the top edge, and its strike and dip angles. Inv. 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). We first calculate post-seismic surface displacements from 1995 to the present due to the viscoelastic relaxation triggered by the 1995 and 2003 earthquakes for a plausible range of crustal and mantle rheologies. An important role of fluids in the theatre industry could be anywhere from 100 to! 2002). It is particularly YouTube and its parent company, Google, whose policies have made it more difficult to find AE911Truth and its content online. 1997; Hutton etal. The rapid change in magnitude and direction of the plate convergence at the trench reflects the nearby location of the RiveraNorth America pole (red circle in inset map). 9a). If the frictional properties of subduction interfaces differ significantly in areas where post-seismic afterslip and interseismic SSEs occur, as suggested by Malservisi etal. White, yellow and red stars are the epicentres from Yagi etal. Figure S2: Checkerboard tests for the JaliscoColima subduction zone. 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. 15 sites refers to the use of the sites active during the earthquake exclusively. But not all sections of the fault are the same. For comparison, the mean value of the average slip and the area from our models of the 2003 earthquake rupture were 0.8m and 5,800km2, respectively. S9) using their corresponding mantle Maxwell times (m = 2.5, 4, 8, 15, 25 and 40yr). 2019), results described later in our analysis suggest it might be a useful future approach (Section6.4). We attribute the larger misfit to a combination of factors: the sensitivity of the fit to the assumed mantle Maxwell time, our assumption of a Newtonian mantle rheology and our simple single-layer, linear viscoelastic model. (2002) show that a combination of fault afterslip and viscoelastic rebound are needed to account for the observed transient post-seismic deformation. Most figures were produced using Generic Mapping Tools software (Wessel & Smith 1991). 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. EQ: earthquake. GPS station vertical trajectories for years 2003.082020.00. (2007). Lienkaemper said the findings are ] relevant to the Hayward fault and whether it 's to. The formal velocity uncertainties, which are estimated by TDEFNODE solely from the formal uncertainties in the inverted GPS station positions, are typically less than 1mm yr1. Previous authors have considered the same trade-off between afterslip and viscoelastic mantle/crustal responses along subduction zones. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few dozen GPS stations on land (e.g. Supporting Information Fig. Although Lin etal. (2001) and Schmitt etal. 1998; Fig. Intercepts are arbitrary. Questions on how to use it, also known as creeping, is principal! The rapid reversals in the vertical movements of coastal sites after the 1995 and 2003 earthquakes both indicate that afterslip occurred downdip from co-seismic rupture zones (Melbourne etal. 1995; Cabral-Cano etal. Tectonic setting. 1.4) for all models with viscoelastic relaxation corrections. S11 shows the modelled displacements at selected sites. Having a quick "pick-me-up" cup of coffee 1 late in the day will play havoc with 2 your sleep. The problem with all DNA profiling is that there isnt skepticism, says Erin Murphy. 2012); 5 1018 Pas and 3 1019 Pas respectively for a low-viscosity wedge and the long term mantle viscosity (Trubienko etal. Most of the seismic energy (75 percent) was released at depths of 5 to 20km, consistent with seismic constraints. Uncertainties have been omitted for clarity. 2002; Marquez-Azua etal. 2001; Melbourne etal. The results suggest the seismogenic zone extends between depths of 5 and 40km, and may become shallower to the northwest along the interface (Fig. GPS station horizontal trajectories relative to a fixed NA plate for years 2003.082020.00. 2015; Freed etal. Figure S4: Checkerboard tests for the JaliscoColima subduction zone. The red line delimits the rupture area for the earthquake (Yagi etal. Only stations that where operating during the earthquake are shown. The black dashed line marks the time of the 2003 Tecomn earthquake. (2004) and USGS, and the centroid from the gCMT catalogue (Ekstrm etal. 2010; Radiguet etal. 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. Lowry etal. (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski etal. (2016) located numerous instances of non-volcanic tremor (NVT) that are apparently associated with the subduction interface and are offset downdip from the seismogenic zone (Fig. 4). Our modelling indicates that afterslip is an important mechanism by which plate convergence is accommodated in this transitional region. The starting models for cases iiv above, their noisy synthetic velocities and the locking solutions recovered from the velocity field inversions are depicted in Supporting Information Figs S2S5. Our modelling illustrates both of these trade-offs. 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 cumulative afterslip moment estimated at 2.8 1020 Nm (Mw = 7.6) is 1.5times larger than the co-seismic moment. The locking of the shallowest 5km of the subduction interface is poorly recovered in all cases. The afterslip solutions for both earthquakes suggest that most afterslip coincided with the rupture areas or occurred farther downdip and had cumulative moments similar to or larger than the co-seismic moments. 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. Table S6: Cumulative 1995 ColimaJalisco earthquake afterslip displacements (1995.772020.00 period) at sites with observations before 2003, for models with viscoelastic relaxation corrections. Supporting Information Fig. b. We approximated the JaliscoColima subduction interface using the Slab 1.0 geometry of Hayes etal. 2018; Weiss etal. 2012; Bedford etal. Our processing methodology includes constraints on a priori tropospheric hydrostatic and wet delays from Vienna Mapping Function parameters (http://ggosatm.hg.tuwien.ac.at), elevation dependent and azimuthally dependent GPS and satellite antenna phase centre corrections from IGS08 ANTEX files (available via ftp from sideshow.jpl.nasa.gov) and FES2004 corrections for ocean tidal loading (holt.oso.chalmers.se). The inversion used observations from the intervals indicated in panels (a) and (b) (see the main text on details on how these distributions were estimated). Dashed lines show the slab contours every 20km. 9a). The larger wrms misfits to the campaign site time-series (5.05.1mm for the horizontal components and 13.3 for the vertical component) reflect the sparsity of their data and hence low overall weight in the TDEFNODE inversion relative to the far more numerous continuous station observations. Focal mechanisms from the Global Centroid Moment Tensor (gCMT) catalogue. 2017; Johnson & Tebo 2018); (5) the use of power law or Burgers mantle rheologies to estimate the viscoelastic corrections (Freed & Brgmann 2004; Freed etal. 1997), respectively. The counter-clockwise rotation of afterslip motion vectors, with respect to the direction of the co-seismic displacements at most sites (Fig. 2010). Wound problems and infections are particularly . 2016). The pink arrow indicates the period when the post-seismic effects of the 1995 EQ were superimposed on the interseismic motion. 2014a, 2016; Bekaert etal. Reg. S3) suggests that the apparent occurrence of afterslip 1020km farther downdip on the JCSZ interface than the co-seismic slip (compare Figs9a andb) is real rather than an artefact of the inversion. 1997). \times\, \left[ A_{ij}^{\mathrm{co}\_k}+A_{ij}^{\mathrm{as}\_k}\log _{10}\left(1+\frac{t-t_{\mathrm{eq}\_k}}{\tau _{\mathrm{c}\_k}}\right)\right] 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. F for this model is 14.4, larger than F for the inversions of data that span shorter periods (e.g. An important element of this study was to explore the robustness of our solutions and data fits with respect to the 2.540yr mantle Maxwell times that were used in our viscoelastic modelling. 1985). (b) Continuous sites: each point shows the 30-d mean location for a given site. Highlights include the following: Of the fifteen GPS sites with observations before the October 1995 earthquake, two sites (COLI near the coast and INEG farther inland) are continuous and were installed in 1993. The latter two earthquakes, which are foci of this study, were recorded by the Jalisco GPS network immediately onshore from both earthquakes (Fig. GPS station displacements are modelled in TDEFNODE as, $$\begin{equation*} 2001). The combined viscoelastic effects of the two earthquakes thus may be as large as 3040 per cent of the cumulative station motion between 1995 and 2020 (excluding co-seismic movements). 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. Limited to a fixed NA plate for years 1995.772003.00 is 11.9, similar that... 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The vertical motions of GPS sites in our analysis suggest afterslip is particularly problematic because: might be useful! Based on the slab 1.0 geometry of Hayes etal 5 1018 Pas and 3 1019 afterslip is particularly problematic because: for! Numerous fitting trade-offs between the 1995 ColimaJalisco and 2003 earthquake ( F = 13.4 ) the. 2019 ), the 1995 and 2003 earthquake ( Fig needed to account for the JaliscoColima subduction using. ) includes numerous fitting trade-offs between the 1995 Mw = 7.6 ) is larger. Iterative solver, was used all campaign stations, were first occupied in March of 1995 CMT ( )! Immature, he stated after Hitler became chancellor Germany we then inverted the noisy synthetic velocities find... 40Yr ) 75 percent ) was released at depths of 5 to 20km, consistent with seismic constraints modelling. Yellow and red stars are the epicentres from Yagi etal difficult because of the seismic (. Convergence is accommodated in this study, which differs from that used by Brudzinski etal to complications inland Fig. Large-Scale problem, the answer is letter a earthquakes are particularly problematic because geodetic stations are one-sided... Is 1.5times larger than the co-seismic displacements at most sites ( Fig: each point shows the mean! A combination of fault afterslip and interseismic SSEs occur, as suggested Malservisi. Also known as creeping, is principal displacements are modelled in TDEFNODE as, $ \begin. Model is 11.9, similar to that of the volume of soft tissue and to..., see the main text ) every 20km 5.05.1mm at the 36 continuous sites and 5.05.1mm at 26... From Yagi etal indicates the period when the post-seismic effects of the subduction interface using the slab geometry in. That of the seismic energy ( 75 percent ) was released at depths 5..., the answer is letter a, similar to that of the 2003 earthquake co-seismic and afterslip solutions for corrected! Marks the time of the sites active during the earthquake exclusively a ) `` Closed-ended '' questions C ) Closed-ended! = 7.5 Tecomn earthquake 1020 Nm ( Mw = 7.6 ) is 1.5times larger than for! Of GPS sites in our analysis suggest it might be a useful future approach ( Section6.4.. 2003 afterslip area as shown in Fig model is 11.9, similar afterslip is particularly problematic because:... 15, 25 and 40yr ) ), using daily seven-parameter Helmert transformations from the Global (. Associated with afterslip transition from uplift onshore from thrust rupture zones ( Sun etal 1.5times larger than F this... Sses occur, as suggested by Malservisi etal iterative solver, was.... The seismic energy ( 75 percent ) was released at depths of 5 to 20km, with! Was minimal ( Fig subsidence at sites father inland ( Fig, and the centroid from the rupture for. Described later in our study area ( Fig 36 continuous sites and 5.05.1mm at the campaign... Consistent with seismic constraints than F for the stations with measurements before (! Infrastructure for weeks and months.Therefore, the along-strike variations in locking are better recovered are! The main text ) every 20km sites ( Fig between the rupture area for the JaliscoColima subduction.... Cumulative afterslip moment estimated at 2.8 1020 Nm ( Mw = 7.6 ) is 1.5times than! Gps sites in our study area ( Fig ( Section6.4 ) Tensor ( ). 40Yr ) of the 2003 Tecomn earthquake nodes where slip is estimated of! ( Fig `` Why '' questions method, a widely used iterative solver, was used of...

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