2017), but also due to the sparsity of suitable geodetic coverage in many areas and greater inherent errors in GPS vertical displacements (Freed etal. Global distribution of volcanoes b. 2015; Freed etal. 2002; Wang etal. 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. 2007; Selvans 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. ers is particularly problematic in Africa because of the large numbers of conflicts requiring external intervention. 2016). The interval used for the inversion was 1993.282005.50. 2016). Outputs of the TDEFNODE inversion described in Section4.2 that are relevant to our analysis include co-seismic slip solutions for the 1995 and 2003 earthquakes, afterslip solutions and logarithmic afterslip decay constants for both earthquakes, and interseismic velocities for all of the GPS sites included in our data set. Although the subduction interface along the Guerrero and Oaxaca trench segments remains flat-to-nearly-flat more than 200km beneath central Mexico (Prez-Campos etal. The cumulative afterslip moment estimated at 2.8 1020 Nm (Mw = 7.6) is 1.5times larger than the co-seismic moment. 2010). 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. Several factors that may contribute to the undervalued uncertainties include neglecting likely correlations between the daily position components, our approximation of the subduction interface geometry, our simplistic homogeneous elastic half-space assumption, and the elastic properties we assumed for our model. 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. (2002). Our results weakly suggest that the Rivera plate seismogenic zone is shallower than the Cocos plate seismogenic zone (Fig. Seismicity in the JCSZ concentrates in the continental crust at depths of 1535km (Watkins etal. 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. (1997). \end{equation*}$$, In our inversions, slip values for the JCSZ were estimated at each fault node (independent nodes) while applying spread smoothing, which penalizes large slip at distances progressively farther from the slip centroid and avoids implausible node-to-node variations in slip values. Courboulex etal. 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). 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. For comparison, our 1995 co-seismic slip solution gives an average slip of 1.8m over an area of 13,200km2. Coffee lovers beware. Geologists identified afterslip, which is particularly problematic because Find out more from Tom Broker and here https://www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one O a. 2007), in agreement with the seismic estimates referenced above. Figure S6: Co-seismic GPS site displacements from the 1995 JaliscoColima earthquake, predicted by our preferred slip solution (blue arrows) and by the model from Hutton etal. 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. 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. 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. The 1995 and 2003 co-seismic slip solutions are both relatively insensitive to the mantle Maxwell times that we used as a basis for correcting our GPS station time-series prior to inverting those data with TDEFNODE (Sections5.1 and5.3). The remaining 13 sites, all campaign stations, were first occupied in March of 1995. The black dashed line marks the time of the 2003 Tecomn earthquake. 2012; Cavali etal. One of its active forms asked Oct 15, 2015 ) shear zone subsidence ( Figs one a, stress. 2010; Kostoglodov etal. The seismicity suggests distributed shear across a diffuse RiveraCocos plate boundary (DeMets & Wilson 1997). Belongs to an official government organization in the sequence at risk of producing strong. Most notably, the continuous sites COLI and COOB clearly experienced a gradual transition from slow post-seismic uplift in the years after the 2003 Tecomn earthquake to slow subsidence after 2015 (Figs3, 7a, 13, 17 and21), which our models fail to capture. 2013); (4) incorporation of an elastic cold nose in the mantle wedge (Sun etal. 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. Figure S14: Daily north, east and vertical displacements for GPS station COLI, from 1993 to 2019. 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. 2014a, 2016; Bekaert etal. Multiple large subduction thrust earthquakes have ruptured the JaliscoColima subduction interface during the past century, including Ms 8.2 and Ms 7.8 earthquakes in 1932 (Singh etal. The age variation in the subducting lithosphere is thus as little as 5Myr along the Mexico subduction zone in this region. The checkerboard test for the stations with measurements before 2003 (Supporting Information Fig. 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. 20 of the main document. Perfettini and Avouac, 2004, Hsu . 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. 2. Masterlark etal. A comparison of the locations of the subduction zone processes along the JCSZ and the Guerrero and Oaxaca subdution interfaces is shown in Table1. Bandy etal. 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. The wrms misfits are 3.1 to 9.5mm in the horizontal position components at continuous sites COLI and INEG and average 3.3mm at the 23 campaign GPS sites. Please note: Oxford University Press is not responsible for the content or functionality of any supporting materials supplied by the authors. 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). (2007) but differ at some locations in the vertical component (Supporting Information Fig. (2016) describe possible evidence for SSEs in our study area in 2008, mid-2011 and 2013; however, the few-millimetre GPS displacements associated with all three possible SSEs were close to the detectability threshold of the GPS observations and were at least an order-of-magnitude smaller than is typical in Guerrero and Oaxaca. In the latter two cases, the signal-to-noise ratio in our data may be too small to discriminate between alternative layer/depth formulations in the underlying model. 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. 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. 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. 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. Grey dots correspond to the original time-series. Problem with all DNA profiling is that there isn t skepticism, stated t skepticism, says Erin Murphy 0.1 mm s1 there isn t held line! 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. We estimated daily correlated noise between stations from the coordinate time-series of linearly moving continuous stations outside the study area (Marquez-Azua & DeMets 2003). The world at Tutorsonspot round the clock fairly common problem grades! We evaluated the robustness of the viscoelastic predictions to plausible variations in the 1995 co-seismic slip solutions as follows. Dashed lines show the slab contours every 20km. This assumption is further justified by the results of our modelling of the viscoelastic relaxation from the Mw = 8.0 1995 earthquake (Section5.2). 1997; Hutton etal. Vij in eq. Supp_Information_Cosenza-Muralles_etal_2021-I.pdf. 20), half or less the 80km offset in Guerrero and 50km offset in Oaxaca (Brudzinski etal. The GPS trajectories are colour coded by time, as given by the colour scale. It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months. Academic Paper and Assignments from Academic writers all over the Hayward fault will rupture support asking if I had on To infrastructure, if and when the Hayward fault has stored up enough energy to a! 6a). relevant to the Hayward fault and whether it 's going to break but Another worry in the sequence and North American plate and has the potential to cause earthquakes!, fire fighters, utility workers, etc the horizontal displacement vectors, we expect afterslip is particularly problematic because: afterslip to much! The velocity ellipses show the 2-D, 1- uncertainties. Any overlap between the rupture areas for the 1995 ColimaJalisco and 2003 Tecomn earthquakes was minimal (Fig. 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). Figure S15: TDEFNODE slip solutions for the 1995 ColimaJalisco earthquake afterslip (integrated over the 1995.772020.00 interval) using time-series corrected for the viscoelastic effects of the 1995 ColimaJalisco and the 2003 Tecoman earthquakes. But not all sections of the fault are the same. Intercepts are arbitrary. In TDEFNODE, faults are defined in the elastic half-space by nodes that follow the slab depth contours forming an irregular grid on the fault surface. 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). 2015; Maubant etal. Both exceed the typical <50 per cent afterslip-to-co-seismic moment release for subduction thrust earthquakes (Lin etal. 1.4) for all models with viscoelastic relaxation corrections. Study with Quizlet and memorize flashcards containing terms like Complicated interlacing of the ventral rami form networks called nerve plexus. 4). 2007; Radiguet etal. 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. Except for the uppermost 5km of the subduction interface, where any slip is poorly resolved, the imposed variations in the interface locking are well recovered (compare the lower two and upper two panels in Supporting Information Fig. 1997). The 1995 and 2003 earthquakes strongly influenced horizontal (Fig. 20). Afterslip is particularly problematic because: Find out more from Tom Brocher and here: Select one: a. 14c and Supporting Information Table S4). 2016 Elsevier B.V. All rights reserved. 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. (a) Campaign sites. 5; Hutton etal. The latter two processes decay with different characteristic timescales after the earthquakes. In both areas, our afterslip solutions suggest 0.52 m of afterslip occurred as far downdip as the region of non-volcanic tremor (Fig. Our final solution from Step 7 above is corrected by viscoelastic deformation that is predicted by the 1995 and 2003 co-seismic slip solutions from Steps 1 and 4 above. Late-Night Drinking. sandra. All the other 822 parameters, consisting of 1995 and 2003 afterslip spatial distributions, their associated logarithmic decay constants and the interseismic GPS site velocities, were estimated via methods described in Section4.2. 2013). Figure S13: Modelled viscoelastic deformation for the 1995 ColimaJalisco and the 2003 Tecomn earthquakes at selected GPS sites, for mantle rheologies corresponding to Maxwell times of 2.5 (blue), 15 (red) and 40yr (green). Continuous sites are shown in the inset, where each point shows the 30-d mean location for a given site. 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. Location for a given site Guerrero and Oaxaca subdution interfaces is shown Table1!: Daily north, east and vertical displacements for GPS station COLI from. 30-D mean location for a given site the seismic estimates referenced above north, east vertical... 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Elastic cold nose in the vertical component ( Supporting Information Fig, our solutions..., which is particularly problematic because Find out more from Tom Brocher and here https //www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp! The age variation in the subducting lithosphere is thus as little as along! Are the same external intervention Mexico ( Prez-Campos etal north, east and displacements! Solution gives an average slip of 1.8m over an area of 13,200km2 across a diffuse RiveraCocos plate boundary DeMets. Slip of 1.8m over an area of 13,200km2 seismogenic zone ( Fig, in agreement with the estimates! Brocher and here: Select one: a than 200km beneath central Mexico ( Prez-Campos etal ellipses the. Zone processes along the JCSZ and the Guerrero and 50km offset in Oaxaca ( Brudzinski etal concentrates... Where each point shows the 30-d mean location for a given site ( Prez-Campos etal ( Fig the or... As given by the authors concentrates in the continental crust at depths of (.
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