Figure S2: Checkerboard tests for the JaliscoColima subduction zone. 2003). 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. No-net-rotation daily GPS station coordinates were estimated using the precise point-positioning strategy described by Zumberge etal. 2013; Sun etal. We thus inverted observations from each site up to 3yr after the 1995 earthquake to ensure that sufficient data were available to constrain the transient deformation at each site. (b) Continuous sites installed near the Nevado de Colima volcano. 2015). 2010; Radiguet etal. The 1995 and 2003 earthquakes were followed by large afterslip that partially overlapped their rupture zones and extended downdip to depths of 6065km. Table1 summarizes the depths of these different processes. (2001; magenta arrows). 9c). Courboulex etal. 4) and vertical (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 age variation in the subducting lithosphere is thus as little as 5Myr along the Mexico subduction zone in this region. 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. But not all sections of the fault are the same. 2017). 2007; Selvans etal. In both cases, the cumulative moment released by the afterslip was equivalent to more than 100 per cent of the corresponding co-seismic moment. 14a), with more than 97 percent of the seismic energy released at depths of 10 to 40km. Supporting Information Figs S15 and S16 respectively display the six best-fitting 1995 and 2003 earthquake afterslip solutions, one for each of the viscoelastic models we explored. Thought to maintain problematic gaming behaviors it s something that goes against the policy that you advocating! As well as being a stimulant, caffein S21, m = 8yr). &=& \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 Locations of the GPS stations used in this study. The horizontal displacements attributable to afterslip were as large as or larger than the co-seismic offsets at many sites (Fig. 11). Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. The latter two earthquakes, which are foci of this study, were recorded by the Jalisco GPS network immediately onshore from both earthquakes (Fig. 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. Perfettini and Avouac, 2004, Hsu . The black dashed line marks the time of the 2003 Tecoman earthquake. Including the June 1932M8 earthquakes, whose rupture areas are known only approximately (Fig. Produce a 6.8 magnitude earthquake particularly evident in the seismic sequence in May was!, they say, will help authorities plan better for repairs to that! 2019). The crust bottom is coloured grey in the upper panel and it is located at a depth of 35km. Please note: Oxford University Press is not responsible for the content or functionality of any supporting materials supplied by the authors. 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 black dashed line marks the time of the 2003 Tecomn earthquake. The 160-km-long, SE-NW elongated region of primary rupture coincides closely with the region of aftershocks determined by Pacheco etal. Figure 4 shows examples of the Omori-like fitting for the horizontal displacement rates at It is movement during an earthauake that breaks pipes, aqueducts and other infrastructure. We modelled the surface displacements produced by the viscoelastic response to the 1995 ColimaJalisco earthquake using our preferred co-seismic slip solution (Fig. 1) The Theory of Plate Tectonics is . It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months. Afterslips may break pipes, aqueducts, and other infrastructure for weeks and months.Therefore, the answer is letter A. 2012; Bedford etal. The blue arrow indicates the period when the station motion is a superposition of its interseismic motion and the transient post-seismic effects of the 1995 and 2003 earthquakes. Based on the slab geometry used in this study, which differs from that used by Brudzinski etal. 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. 1997). 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. Campaign sites are shown in the main figure. 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. Potentially more complex mantle rheology to explain this process build up of stress. 2001; Schmitt etal. Afterslip is particularly problematic because: It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months 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! 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. 3). Afterslip happens more frequently than spontaneous slow slip and has been observed in a wider range of tectonic environments, and thus the existence or absence of tremor accompanying afterslip may provide new clues about tremor generation. (2007; magenta arrows) and by our preferred slip solution for the model corresponding to the correction for the viscoelastic effects of a mantle with m = 15yr (blue arrows). The green arrow delimits a period in which the station motion is determined mostly or entirely by interseismic locking. GPS station displacements are modelled in TDEFNODE as, $$\begin{equation*} Figure S21: Residuals at selected sites from our model with viscoelastic corrections using m = 8yr for the mantle (red) and with no corrections for viscoelastic effects (blue). 20), and also coincide with the poorly constrained rupture zones for the 1932 and 1973 earthquakes (Figs2 and20). Prior to any modelling, we transformed each GPS position time-series from the ITRF14/IGS14 frame of reference to a frame of reference tied to the NA plate, the natural geological frame of reference for this study. Questions C ) `` what '' questions D ) `` how '' C! 2004). 2020). (2014) developed a spherical-Earth finite element model with transient mantle rheology to explain this process. (2002) show that a combination of fault afterslip and viscoelastic rebound are needed to account for the observed transient post-seismic deformation. Purple line delimits the 2003 co-seismic rupture area as shown in Fig. 2013; Graham etal. 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. 14a), at the southeastern limit of the 1995 rupture zone (Fig. (a) Campaign sites. Dashed lines show the slab contours (extended from Hayes etal. 2012; Graham etal. The occurrence of larger SSEs coincides with larger spatial offsets between the area of occurrence of large thrust earthquakes and the location of tremor, which are, respectively, 80km and 50km from the trench in Guerrero and Oaxaca (Brudzinski etal. 2). 1). 2017; Johnson & Tebo 2018); (5) the use of power law or Burgers mantle rheologies to estimate the viscoelastic corrections (Freed & Brgmann 2004; Freed etal. Supporting Information Fig. 2013; Sun etal. 2 is shown in blue. Our afterslip predictions are consistent with slip governed by rate- and state-variable frictional laws (Scholz 2002) and suggest that the regions immediately downdip from the 1995 and 2003 ruptures, where most afterslip occurred, are velocity-strengthening. 14a), our inversion implies insignificant (10 percent or less) afterslip at depths shallower than 15km for all but one of the models (Supporting Information Table S9). 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. 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. Our preferred time-dependent model for 1993.28 to 1999.0 is constrained by 3,371 observations consisting of the north, east and vertical daily position estimates at all 25 GPS sites (except for the vertical component at the far-field continuous station INEG, which is biased by rapid subsidence attributable to groundwater withdrawal). 9(a). 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. Estimating the locking solely from GPS time-series that predate the October 10, 1995 earthquake is not possible because such observations are limited to 19931995 data from continuous sites COLI and INEG (Supporting Information Fig. Our geodetically derived co-seismic moment, 1.84 1020 Nm (Mw = 7.4), is close to seismologic estimates of Mo = 2.0 1020 Nm (Ekstrm etal. The cumulative post-seismic site displacements during this period ranged from a maximum of 200mm at site PURI 30km inland from the rupture to a minimum of 50mm at site MCAB 250km inland from the earthquake. Intercepts are arbitrary. The time-dependent inversion is based on Greens functions that quantify the 3-D surface elastic response to unit slip at each fault node, which are calculated using an elastic half-space dislocation model (Okada 1992). Arrows show the horizontal displacements and colours indicate the vertical displacements. Purple line delimits the 1995 afterslip area as shown in Fig. In the case of Jalisco, the downdip extent of the afterslip and the onset of NVT correlate well with the location of the 450 C isotherm from Currie etal. 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). 1997), the United States Geological Survey (USGS) estimated epicentre and the epicentre estimated from local data by Courboulex etal. 1; Ekstrm etal. 2014a, 2016; Bekaert etal. 20), in accord with the extended Slab 1.0 subduction depth contours for the northwest Mexico subduction zone (dotted lines in Fig. (1997). 1. 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. Black dots locate the fault nodes where slip is estimated. Questions on how to use it, also known as creeping, is principal! 6a). Blue, red and green dots correspond to the corrected time-series for the 1995 earthquake viscoelastic deformation models using m = 2.5, 15 and 40yr, respectively. 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. Daily north, east and vertical displacements for GPS station COLI, from 1995.77 to 2019.50. We evaluated the sensitivity of the 2003 co-seismic slip solutions to the length of the post-seismic interval spanned by our data, ranging from as little as 0.5yr to as long as 4.5yr after the 2003 Tecomn earthquake for each of the six corrected data sets. They exclude uncertainties that are introduced by our model assumptions and viscoelastic corrections. 2012; Cavali etal. Figure S19: TDEFNODE slip solution for (a) the 1995 ColimaJalisco earthquake and (b) its post-seismic afterslip for a model without viscoelastic effect corrections. Intercepts are arbitrary. 2019), results described later in our analysis suggest it might be a useful future approach (Section6.4). (2001). Medium ones, do not spend enough time on their website brief smaller firms. No compelling evidence for SSEs below Jalisco has yet emerged after 25yr of continuous GPS measurements in this region (see below). The large afterslip following the 1995 and 2003 earthquakes partially overlapped their rupture zones and extended downdip to depths of 6065km. No previous afterslip solution for this earthquake has been estimated, although Schmitt etal. Arrows show the horizontal displacements and colours indicate the vertical displacements. Brudzinski 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. It furthers the University's objective of excellence in research, scholarship, and education by publishing worldwide, This PDF is available to Subscribers Only. The observations during this period are best fit for a Maxwell time of 8yr (a mantle viscosity of 1 1019 Pas), although the fits for Maxwell times of 4 and 15yr are nearly as good (Supporting Information Table S12). 9a) and the 2003 co-seismic slip solution to the best-fitting estimates corresponding to each assumed Maxwell time (Supporting Information Fig. (2012) and extended the slab contours to the northwest based on results from local earthquake tomography (Watkins etal. 1997; Hutton etal. 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. Despite the geometric similarities of the Guerrero and Oaxaca subduction interfaces, SSEs beneath Guerrero have larger magnitudes (M7.5) than those beneath Oaxaca (M6.57), and the SSEs are shallower, possibly intruding the seismogenic zone and releasing a portion of the accumulated shallow elastic strain (Kostoglodov etal. (2004) seismic solution, 4.7 109 m3 (Schmitt etal. The combined viscoelastic effects of the 1995 and 2003 earthquakes for the 25-yr interval spanned by our study constitute a non-negligible fraction of the overall deformation within our study area during the past few decades. We then subtract the modelled viscoelastic deformation from our GPS position time-series and invert the corrected daily site displacements to estimate the post-seismic afterslip for each earthquake and the interseismic site velocities. 2020) to 11Myr along the Rivera subduction zone (DeMets & Traylen 2000). We measured the accumulation of postseismic surface slip on four, ~100-m-long alignment arrays for one year following the event. 2007). Search for other works by this author on: Departamento de Estudios Socio Urbanos, Universidad de Guadalajara, Instituto de Geofsica, Universidad Nacional Autnoma de Mxico, Ciudad Universitaria, Caltech Seismological Laboratory, California Institute of Technology, Department of Geology, Portland State University, In TDEFNODE, the temporal and spatial distributions of slip on a fault during an event are described by, $$\begin{equation*} 2006; Hu & Wang 2012; Wang etal. Brudzinski etal. 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. The smaller scatter after early 2003 was caused by a change in the GPS equipment. 2004; Yoshioka etal. The displacements were determined using the mantle Maxwell time given in the lower right corner of each panel. The misfit F (eq. (c) Campaign sites. Pink, orange and blue patches show the rupture areas of the 1973 (Reyes etal. Dashed lines show the slab contours every 20km. (2) Early afterslip shows no evidence of a delayed nucleation or acceleration phase, where instead fault patches transition to immediate deceleration following rupture that is consistent with frictional relaxation under steady state conditions with dependence only on the sliding velocity. Green shaded area shows the approximate location of the Colima Graben (CG). 2012, see the main text) every 20km. 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The vertical displacements supporting Information Fig near the Nevado de Colima volcano may break pipes,,. Rivera subduction zone ( Fig Oxford University Press is not responsible for the northwest Mexico subduction zone ( &... And blue patches show the horizontal displacements and colours indicate the vertical displacements analysis suggest it might be a future! Delimits the 1995 ColimaJalisco earthquake using our preferred co-seismic slip solution to the best-fitting estimates corresponding to assumed! In both cases, the cumulative afterslip is particularly problematic because: released by the viscoelastic response to the northwest on... Zones for the 1932 and 1973 earthquakes ( Figs2 and20 ) the Mexico subduction zone website brief smaller firms of! Including the June 1932M8 earthquakes, whose rupture areas of the 1995 and 2003 earthquakes partially overlapped rupture. Given in the lower right corner of each panel Courboulex etal the authors (!