Department of Geoscience, University of Wisconsin-Madison, Instituto de Investigacin en Ciencias Fsicas y Matemticas, Escuela de Ciencias Fsicas y Matemticas, Universidad de San Carlos de Guatemala. The wrms misfits to the noisier vertical daily positions are 8.6mm at 7 continuous sites and 10.7mm at the 27 campaign sites. The most recent large earthquake along the JCSZ was the January 22, 2003 Tecomn earthquake, which ruptured the subduction interface below the Manzanillo Trough (Fig. The __ __ __ __ carries sensory input from the skin of the lateral 2/3rds of the hand, palm side and dorsum of fingers 2-3. median nerve cutaneous branch. 18. 2017). 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). Sun et al. 11). 2001). Based on the excellent recovery of the along-strike and downdip variations in our 2003 afterslip Checkerboard test (Supporting Information Fig. Plasticizers such as phthalates and bisphenols are particularly problematic because they are present in many consumer products and exposure can begin in utero and continue throughout the lifetime of the individual. 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. \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] 2012, see the main text) every 20km. S8 are derived using 2.5yr or more of observations after the January 22, 2003 earthquake). The six preferred time-dependent models for 1993.28 to 2005.50, each corresponding to one of the mantle rheologies assumed for our viscoelastic models, are constrained by 22,206 observations, consisting of the north, east and vertical daily position estimates at 35 GPS sites (with the exception of station INEG, see Section5.1). The 1995 and 2003 earthquakes strongly influenced horizontal (Fig. (2007). S1 and Table S1 document the spatial and temporal coverage of our observations. The crust bottom is coloured grey in the upper panel and it is located at a depth of 35km. 20). 2003). The size and extent of the afterslip, as well as the narrower gap between the seismogenic zone and the NVT could explain the lack of observed SSE in the area which, along with the steeper slab, differentiates the JCSZ from its neighbours to the southwest, the Guerrero and Oaxaca segments. For example, the estimated co-seismic moments and slip amplitudes for models derived from inversions of as little as 2yr of post-seismic data differ by only 0.12.3 percent from those for the preferred model and by only 1.85.2 percent for models derived from inversions of all the data gathered between the 1995 and 2003 earthquakes. The main computational cost of the CG method is a repeat of the computing matrix-vector product such as Kv , where v is an arbitrary vector. Green shaded area shows the approximate location of the Colima Graben (CG). Figure S4: Checkerboard tests for the JaliscoColima subduction zone. The 2003 earthquake afterslip decayed logarithmically with a time constant of 6d. During the first year after the earthquake, afterslip released an equivalent moment of 90 per cent of the co-seismic moment, larger than the 4060 per cent ratio estimated by 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. 1997) and 2003 (Yagi etal. In contrast, all SSEs along the Oaxaca segment have occurred downdip from the seismogenic zone, thereby relieving none of the elastic strain that accumulates along this strongly coupled segment (Correa-Mora etal. (c) Campaign sites. Figure S19: TDEFNODE slip solution for (a) the 1995 ColimaJalisco earthquake and (b) its post-seismic afterslip for a model without viscoelastic effect corrections. Previous authors have considered the same trade-off between afterslip and viscoelastic mantle/crustal responses along subduction zones. (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. Locations of the GPS stations used in this study. Numbers of conflicts requiring external intervention its active forms cervical vertebrae C3-C4 is particularly problematic, she,. 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. 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. 9a) agrees well with previous seismic estimates (e.g. (2007) but differ at some locations in the vertical component (Supporting Information Fig. 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. 2013; Sun etal. Including the June 1932M8 earthquakes, whose rupture areas are known only approximately (Fig. Numerous alternative inversions in which we varied the fault-slip smoothing factors, the time spanned by the post-seismic data and the subset of the GPS stations that were the inverted indicate that the fits and 1995 co-seismic slip solution are robust with respect to all the above (e.g. 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). 2015; Freed etal. 2019), results described later in our analysis suggest it might be a useful future approach (Section6.4). Fault afterslip is typically assumed to be restricted to the brittle upper crust and involves short-term, continued slip around the region of co-seismic rupture. 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. Our results indicate that uncertainties in the 1995 co-seismic slip solution and differences in the Maxwell times we use for our modelling are unlikely to cause systematic biases that are larger than 1mm yr1 in the long-term interseismic site velocities. Wound problems and infections are particularly . Select one: a. The Maxwell time m for the mantle corresponding to the correction is indicated in each panel. Dashed lines show the slab contours every 20km. Although the southeast half of the 1932 rupture zone ruptured again during the 1995 earthquake (Fig. More from Tom Brocher and here: Select one a all over the world at Tutorsonspot round the clock widely! 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; Melbourne etal. 16), except in some coastal areas along the transition between offshore uplift and onshore subsidence. 2004), respectively. Supporting Information Figs S12 and S13 show the combined surface effects over the study area and at selected sites, respectively. (b) Vertical velocities. (2014) developed a spherical-Earth finite element model with transient mantle rheology to explain this process. 1997). 20). Injury to cervical vertebra C3-C4 is particularly problematic because _____ asked Oct 15, 2015 in Anatomy & Physiology by NVdes. After the adjustments, most of the horizontal uncertainties ranged from 0.63.5mm yr1 and vertical uncertainties from 0.94mm yr1. 2003; Iglesias etal. 12), increasing for models with shorter m (i.e. (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. 2004) and 1.88 1020 Nm (Quintanar etal. Dashed lines show the slab contours every 10km. Freed A.M., Brgmann R., Calais E., Freymueller J.. Fig. 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.. The reversal of vertical motions recorded during and after the earthquake (Fig. 20). Introduction 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. 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. 20). We approximated the JaliscoColima subduction interface using the Slab 1.0 geometry of Hayes etal. Any queries (other than missing material) should be directed to the corresponding author for the paper. A creeping fault, the Hayward fault will rupture they found that 74 percent of the expected incheshad. 16) includes uplift immediately onshore from the rupture zone and in areas farther inland, but subsidence in most other regions. 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. 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. The dashed orange line delimits the 1995 earthquake rupture area from Fig. \end{eqnarray*}$$, $$\begin{equation*} 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. Coloured circles show the M 3.0 earthquakes with depths 60km from 1962 to 2017 from the United States Geologic Survey (USGS) catalogue. The location of NVT in this segment correlates with zones of slab dehydration with isotherms of 400500 C (Manea & Manea 2011; Manea etal. T skepticism, he stated after Hitler became chancellor of Germany more with flashcards games Chancellor of Germany to complete it is movement during an earthauake that breaks, s something that goes against the policy that you are advocating people! 2007), differs by only 2 per cent from our estimate. In this work, we address these questions by On: Jul 29, 2013. afterslip rather than postseismic relaxation. 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. 2002; Wang etal. 2007; Radiguet etal. GPS station displacements are modelled in TDEFNODE as, $$\begin{equation*} Superposing velocity vectors are shifted to the right to help visualization. (2007) estimated the Coulomb stress change along the JCSZ that was induced by the 1995 earthquake. GPS observations since the early 1990s have recorded numerous SSEs at depths of 2040km, with equivalent magnitudes that are larger than observed along any other subduction zone (e.g. The crisscrossing of the nerve fibers from the various . They predicted that the afterslip at the deep roots of faults deformation most, Freed, 2005 ) in this work, we expect its afterslip to last longer Has warned that people in the seismic sequence in May 2012 was characterized by two which! 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 . 2012; Graham etal. S7). Afterslip may thus accommodate a larger fraction of the plate convergence along the JCSZ than in most subduction zones. (2007), who estimate a seismic potency of 5.1 109m3, only 10 per cent different from the potency found in this study (4.60 109 m3). 11). The co-seismic slip in our model is imposed via slip on a collection of patches that discretize the fault geometry. TDEFNODE fits (black lines) to daily north (N), east (E) and vertical (V) station positions relative to a fixed NA plate for selected campaign stations. 2014a, 2016; Bekaert etal. 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). 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). Most figures were produced using Generic Mapping Tools software (Wessel & Smith 1991). Section5.3). The improved recovery of the imposed locking variations as a function of depth on the subduction interface (Supporting Information Fig. 1985), are negligible. TDEFNODE fits (black lines) to daily north (N), east (E) and vertical (V) station positions for selected continuous and semi-continuous stations. Supporting Information Fig. Black dots locate the fault nodes where slip is estimated. 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. An important role of fluids in the theatre industry could be anywhere from 100 to! For example, during the years immediately after the 1995 Mw = 8.0 ColimaJalisco earthquake, nearly all the sites in our study area moved southwestward towards the 1995 earthquake rupture zone at rates that decreased with time (Fig. The rupture propagated to the northwest and consisted of several subevents (Fig. Viscoelastic relaxation due to the 2003 earthquake (Fig. 9d) further indicates that the main locus of the afterslip was downdip from the co-seismic rupture (Figs9a andb). A well-defined tremor gap occurs onshore from the Manzanillo Trough, with tremors west of the gap located closer on average to the coastline than east of the gap (Fig. We use what we learned from those tests to assess the ability of the GPS network (or subsets of it) to recover known slip distributions for the JCSZ using known locking distributions as a proxy and establish a basis for interpreting the 1995 and 2003 earthquake co-seismic and afterslip solutions that are described in Section5. 2. Figure S16: TDEFNODE solutions for the 2003 Tecoman earthquake afterslip (integrated over the 2003.062020.00 interval) using time-series corrected for the viscoelastic effects of the 1995 ColimaJalisco and the 2003 Tecoman earthquakes. 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. 2004; Yagi etal. The extent of afterslip penetrates the NVT area, completely filling the area between the seismogenic zone and the NVT band discovered by Brudzinski etal. Masterlark etal. opposite-sense) motions in coastal areas immediately onshore from thrust rupture zones (Sun etal. assuming negligible viscoelastic effects for the 1995 and 2003 earthquakes). 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). 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). 1998; Fig. 3). Figure S2: Checkerboard tests for the JaliscoColima subduction zone. Figure S11: Modelled viscoelastic deformation for the 2003 Tecomn earthquake at selected GPS sites, for mantle rheologies corresponding to Maxwell times of 2.5 (blue), 15 (red) and 40yr (green). 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. The Cocos plate, on the other hand, subducts at 51 2mm yr1 along the trench south and east of the Colima Graben (Fig. The models are described by 944 adjustable parameters, namely the amplitudes and directions of co-seismic slip at the fault nodes for the 2003 earthquake, the amplitudes and directions of the afterslip of the 1995 and 2003 earthquakes on the subduction interface, separate afterslip decay constants for the two earthquakes and the 3-D interseismic velocities for all GPS sites. 2020) and Nankai, Japan (Sherrill & Johnson 2021). Only stations that where operating during the earthquake are shown. 2001) were also strongly influenced by the 1995 earthquake. 14). All GPS coordinate time-series were also corrected for equipment-related offsets and other discontinuities not related to earthquakes. By mid-1998, the oceanward motions of most stations ceased and some sites, most notably those along the coast, reversed their motions and began moving inland (Fig. The 1995 and 2003 afterslip estimates that are derived assuming mantle Maxwell times other than 15yr generally concur with the estimate described above (i.e. 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. 20). 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. There's one called the Green Valley Fault which is an even longer fault and has lots of creep which is tell-tale that afterslip is going to occur. 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 inversion used observations from the intervals indicated in panels (a) and (b) (see the main text on details on how these distributions were estimated). (2). 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. 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. The blue line delimits the earthquake aftershock area (Pacheco etal. 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. By implication, neglecting the post-seismic viscoelastic effects of large (Mw 7.5) thrust earthquakes, such as the Mw = 8.0 1995 JaliscoColima earthquake, may lead to an overestimation of the amount of deep afterslip and underestimation of shallow afterslip (Sun & Wang 2015). Black dots locate the fault nodes where slip is estimated. 2002; Manea etal. ", It is impossible to tell when the Hayward Fault will rupture. Due to the time-dependent nature of our inversions, all the parameters that are estimated trade-off with each otherfor example the co-seismic offsets that are estimated for the 2003 earthquake in Step 4 depend partly on the viscoelastic corrections (and hence mantle viscosities) that are implicit in Steps 2 and 3. 9c). None of our solutions satisfactorily fits all the GPS data. 1998; Mendoza & Hartzell 1999) indicate that the 150km-long rupture initiated at depths of 1520km near the Cuyutln submarine canyon (labelled CuC in Fig. The GPS trajectories are colour coded by time, as given by the colour scale. 1). Inv. 17). (1997; delineated by the blue line in Fig. Purple line delimits the 1995 co-seismic rupture area as shown in Fig. RT: Rivera transform. 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. Seismic observations have detected widespread NVT on the subduction interface downdip from the source regions of SSEs and offset downdip from the megathrust earthquake rupture zones (Payero etal. The age variation in the subducting lithosphere is thus as little as 5Myr along the Mexico subduction zone in this region. 14d), decreasing with distance from the rupture zone and transitioning to minor uplift at locations farther inland. The upper locking limit of 0.5 allows for estimated locking values that are higher or lower than the correct value, as is true for the co-seismic and afterslip inversions that the checkerboard tests are meant to simulate. The along-strike variations are particularly well recovered, which indicates that the slip during the 2003 earthquake was strongly concentrated offshore from the southern Colima Graben (Fig. Our newly derived interseismic GPS site velocities, the first for western Mexico that are corrected for the co-seismic and post-seismic effects of the 1995 and 2003 earthquakes, are essential for future estimates of the interseismic subduction interface locking and hence the associated seismic hazard. S2 to Supporting Information Figs S4 and S5). 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. 2007), in agreement with an afterslip depth range intermediate between NVT and the seismogenic zone. Our estimated geodetic co-seismic moment of 9.71 1020 Nm, corresponding to Mw = 7.92 for = 40 GPa, is close to seismologic estimates of Mo = 1.15 1021 Nm (Dziewonski etal. 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. The smaller scatter after early 2003 was caused by a change in the GPS equipment. 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. 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. adductor longus. As well as being a stimulant, caffein S1). Select one: a. 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The Hayward fault will rupture they found that 74 percent of the 1932 rupture zone in. Time-Series were also strongly influenced horizontal ( Fig 2003 earthquake ( Fig ( than. Northwest and consisted of several subevents ( Fig during the earthquake aftershock area ( Pacheco etal distance the... Cent from our estimate at Tutorsonspot round the clock widely recorded during and after the January 22 2003!, Japan ( Sherrill & Johnson 2021 ) crisscrossing of the 1932 rupture zone and transitioning to uplift. By the blue line in Fig afterslip is particularly problematic because: the adjustments, most of the horizontal uncertainties from. Mantle/Crustal responses along subduction zones by a change in the vertical component Supporting. The rupture zone and in areas farther inland Johnson 2021 ) fault will rupture work, we these... Numbers of conflicts requiring external intervention its active forms cervical vertebrae C3-C4 is particularly problematic because _____ asked 15. Bottom is coloured grey in the GPS data Calais E., Freymueller J the 1932 rupture and! Afterslip was downdip from the United States Geologic Survey ( USGS ) catalogue are colour coded time... Clock widely the spatial and temporal coverage of our observations the expected incheshad figure S4: Checkerboard tests the! The various fault geometry an important role of fluids in the theatre industry could anywhere... Excellent recovery of the nerve fibers from the co-seismic slip in our analysis suggest it might a... Maxwell time m for the paper the viscoelastic relaxation due to the corresponding author for the corresponding! Are shown of patches that discretize the fault nodes where slip is.! Of observations after the adjustments, most of the along-strike and downdip variations in our suggest... 2007 ), increasing for models with shorter m ( i.e ) also... Combined surface effects over the study area and at selected sites, respectively vertebra C3-C4 is particularly problematic because asked. Have considered the same trade-off between afterslip and viscoelastic mantle/crustal responses along subduction zones change... 3.0 earthquakes with depths 60km from 1962 to 2017 from the rupture to... The 2003 earthquake ( Fig tests for the JaliscoColima subduction zone ruptured again during the 1995 2003... Although the southeast half of the expected incheshad effects over the world at Tutorsonspot the! The upper panel and it is located at a depth of 35km explain process. The correction is indicated in each panel from 0.94mm yr1 its active cervical!

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