Select one: a. 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. 2006; Hu & Wang 2012; Wang etal. 1979). 20). During the first 3.5yr after the earthquake, afterslip released an equivalent of 80 per cent of the co-seismic moment, comparable to the afterslip versus co-seismic moment release ratio of 70 per cent reported by Hutton etal. 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! Black dots locate the fault nodes where slip is estimated. . White, yellow and red stars are the epicentres from Yagi etal. The maximum horizontal post-seismic displacements were a few tens of millimetres, 25 percent of those for the larger-magnitude 1995 earthquake (Figs4 and5). 2012, see the main text) every 20km. In general, our predictions reproduce the characteristic post-seismic subsidence and horizontal convergence of areas directly above the downdip edge of the rupture (Sun & Wang 2015). 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. 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 co-seismic slip for all six solutions is concentrated below the Manzanillo Trough and the earthquake moments vary by less than 7.6 per cent relative to an average Mo of 1.98 0.07 1020 Nm for all six models (Supporting Information Table S4), corresponding to Mw = 7.47.5. 1.3) and weighted root mean square (wrms) error (eq. The black dashed line marks the time of the 2003 Tecoman earthquake. 2013; Graham etal. Black dots locate the fault nodes where slip is estimated. 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 Maxwell time m for the mantle corresponding to the correction is indicated in each panel. sandra. 20) support this hypothesis. 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. 10 shows the fits of our time-dependent model to the positions for all 15 GPS sites with measurements that span the 1995 earthquake. 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). (2002) show that the observed station motions are even better approximated via a superposition of linear elastic shortening from locking of the shallow subduction interface, logarithmically decaying fault afterslip and post-seismic viscoelastic flow. Black dots locate the fault nodes where slip is estimated. 1997). The large misfit F values of our solutions (>13) are symptomatic of an undervaluation of the data uncertainties. 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. Inversions of seismic waveforms for the 1995 and 2003 earthquakes yield slip solutions with depths shallower than 30km (Sections 5.1 and 5.3), consistent with the depth ranges of our GPS-derived co-seismic slip solutions. Co-seismic subsidence is predicted at most sites (Fig. Overlap of post-seismic afterslip regions and SSE and tremor zones has been observed in other subduction zones such as Cook Inlet, Alaska (Huang et al. Horizontal displacements in most of our study area are in the southwest direction, towards the rupture, except in some coastal areas along the transition between offshore uplift and onshore subsidence (Fig. Summary. 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). correlations) between their adjustable parameters (e.g. 1 However, these figures do not include the marketing content online, in print, at the movies, in video games, or at school. But not all sections of the fault are the same. (2002) from their modelling of continuous measurements at site COLI. 1997). 2008; Radiguet etal. 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. The vertical motions of GPS sites in our study area (Fig. 2001; Schmitt etal. This assumption is further justified by the results of our modelling of the viscoelastic relaxation from the Mw = 8.0 1995 earthquake (Section5.2). 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. Synonym Discussion of problematic. 6c), and some sites significantly northwest of the rupture zone moving away from it (TENA, CHAM, MILN and PORT). 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. (b) Continuous sites: each point shows the 30-d mean location for a given site. Panels (c) and (d) respectively show the horizontal and vertical site motions that are predicted by the co-seismic and afterslip solutions from panels (a) and (b) at sites active during the earthquake for panel (c) and sites active between 1995 and 2003 for panel (d). 12), increasing for models with shorter m (i.e. S6). Table S10: Site velocities for all models with viscoelastic relaxation corrections. Coloured circles show the M 3.0 earthquakes with depths 60km from 1962 to 2017 from the United States Geologic Survey (USGS) catalogue. 15 sites refers to the use of the sites active during the earthquake exclusively. White, yellow and red stars are the epicentres from Yagi etal. White, yellow and red stars are respectively the epicentres from Courboulex etal. The latter two processes decay with different characteristic timescales after the earthquakes. By 22.5yr after the earthquake, the sense of vertical motion at most sites reversed, likely due to the superposition of time-varying vertical effects of fault afterslip and viscoelastic rebound on steady interseismic uplift and/or subsidence at each site. opposite-sense) motions in coastal areas immediately onshore from thrust rupture zones (Sun etal. Figs9(b) and14(b) respectively show the best-fitting 1995 and 2003 earthquake afterslip solutions derived from the GPS positions that were corrected by the representative m = 15yr viscoelastic model. Any overlap between the rupture areas for the 1995 ColimaJalisco and 2003 Tecomn earthquakes was minimal (Fig. (2004) and the USGS (stars in Fig. 2004). s(x,w,t)=AX(x)W(w)S(t) 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. Brudzinski etal. 2004; Suito & Freymueller 2009; Hu & Wang 2012; Kogan etal. We evaluated the robustness of the viscoelastic predictions to plausible variations in the 1995 co-seismic slip solutions as follows. The velocity ellipses show the 2-D, 1- uncertainties. 2004). 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. (2001). We then inverted the corrected GPS position time-series via TDEFNODE while fixing the 1995 co-seismic slip solution to the same preferred estimate as was used to drive the viscoelastic model (Fig. The afterslip solutions that are associated with longer Maxwell times, and hence smaller-magnitude viscoelastic deformation, display little or no shallow afterslip and large-magnitude, deep afterslip (Supporting Information Figs S15 and S16). Figure S14: Daily north, east and vertical displacements for GPS station COLI, from 1993 to 2019. Most figures were produced using Generic Mapping Tools software (Wessel & Smith 1991). 2013; Sun & Wang 2015; Freed etal. Injury to cervical vertebra C3-C4 is particularly problematic because _____ asked Oct 15, 2015 in Anatomy & Physiology by NVdes. 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. 2015). 2010). Surgery for pelvic and acetabular fractures in this population is particularly problematic because conventional treatment often requires large surgical exposures. 1997; Escobedo etal. 14b). 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. 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. Table S4: Co-seismic displacements from the 2003 Tecomn earthquake at GPS sites active during the earthquake. 2001). Including the June 1932M8 earthquakes, whose rupture areas are known only approximately (Fig. 9a) and the 2003 co-seismic slip solution to the best-fitting estimates corresponding to each assumed Maxwell time (Supporting Information Fig. The misfit, $$\begin{eqnarray*} (2004) and USGS, and the centroid from the gCMT catalogue (Ekstrm etal. The data underlying this paper are in the public domain and are available at http://unavco.org, with the exception of GPS sites COLI and INEG. None of our solutions satisfactorily fits all the GPS data. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few dozen GPS stations on land (e.g. 20 are reliable, although the updip and downdip limits of each are still uncertain. 2007), in agreement with the seismic estimates referenced above. 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. adductor longus. Figure S19: TDEFNODE slip solution for (a) the 1995 ColimaJalisco earthquake and (b) its post-seismic afterslip for a model without viscoelastic effect corrections. UNAVCOs initial support for TLALOCNet (now part of NOTA) was performed under EAR-1338091 and is currently supported by the National Science Foundation and the National Aeronautics and Space Administration under NSF Cooperative Agreement EAR-1724794. 2015; Freed etal. The sun and moon exert a gravitational tug on Earth that stretches and compresses crustal rocks. Table S9: Downdip distribution of afterslip for all models corrected for viscoelastic relaxation in percentage of total afterslip moment release at the indicated depth intervals. 2020) to 11Myr along the Rivera subduction zone (DeMets & Traylen 2000). 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 improved recovery of the imposed locking variations as a function of depth on the subduction interface (Supporting Information Fig. Plus or minus 100 or so years, '' he says slip ( ). 2012; Cavali etal. 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). 2 and Supporting Information Fig. We use RELAX 1.0.7 (Barbot & Fialko 2010a, b; Barbot 2014), published under the GPL3 license, to simulate the co-seismic stress changes imparted to the surrounding medium by co-seismic slip and the spatiotemporal evolution of surface deformation resulting from the relaxation of viscoelastic rheologies underlying an elastic upper crust. 2001). 9d). 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. 2015); (7) the use of lateral variations in the thickness of the crust; (8) additional layering in the upper crust and mantle (Wiseman 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. 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. Black dots locate the fault nodes where slip is estimated. 20), and also coincide with the poorly constrained rupture zones for the 1932 and 1973 earthquakes (Figs2 and20). B Cosenza-Muralles, C DeMets, B Mrquez-Aza, O Snchez, J Stock, E Cabral-Cano, R McCaffrey, Co-seismic and post-seismic deformation for the 1995 ColimaJalisco and 2003 Tecomn thrust earthquakes, Mexico subduction zone, from modelling of GPS data, Geophysical Journal International, Volume 228, Issue 3, March 2022, Pages 21372173, https://doi.org/10.1093/gji/ggab435. introduction-to-social-work-and-social-welfare ; 0 Answers. The fits to the campaign site data for all three of these Maxwell times are clearly superior to the fits for a model without any viscoelastic correction, particularly at the subset of the sites that were located directly onshore from the earthquake (e.g. White, yellow and red stars are the epicentres from Courboulex etal. They exclude uncertainties that are introduced by our model assumptions and viscoelastic corrections. Thus, we derived those solutions by inversion of time-series with only a few years of post-seismic data as explained below. 8) equates to respective horizontal and vertical dimensions of 1280km1280km and 640km. 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. No compelling evidence for SSEs below Jalisco has yet emerged after 25yr of continuous GPS measurements in this region (see below). 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. The results suggest the seismogenic zone extends between depths of 5 and 40km, and may become shallower to the northwest along the interface (Fig. 20). 9c). 2005), may constitute a mechanical barrier to along-strike rupture propagation on the subduction interface (Schmitt etal. AUTA, AYUT and GUFI) increased, whereas most inland sites subsided. 2007), in agreement with the seismic results. 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. 2003). 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. 2015; Maubant etal. Positions are progressively shifted to the right to help visualization. In the case of co-seismic slip estimates, we adapted this collection of slip patches as input for our forward modelling of the viscoelastic response (Section4.1). 2014a, 2016; Bekaert etal. It is important to note that advertising and marketing can serve a useful purpose for children. Marquez-Azua etal. 2004) earthquakes, respectively. (b) Continuous sites installed near the Nevado de Colima volcano. The postseismic observations favor a ramp-flat structure in which the flat angle should be lower than 10. 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. 2007), was the first large rupture of the JCSZ segment since 1932. 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. Figure S4: Checkerboard tests for the JaliscoColima subduction zone. 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. 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