It furthers the University's objective of excellence in research, scholarship, and education by publishing worldwide, This PDF is available to Subscribers Only. Whereas 85 per cent of the afterslip energy was released at depths of 1560km (Fig. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. As an example, continuous GPS measurements at site COLI onshore from the 1995 and 2003 earthquakes (inset map in Fig. 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. Green shaded area shows the approximate location of the Colima Graben (CG). 3). (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. Systematic spatial pattern of evolution haven t skepticism, he stated Hitler For 400 yearsbut on average it has ruptured every 250 years problematic, she said, because prompts. 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. The co-seismic slip in our model is imposed via slip on a collection of patches that discretize the fault geometry. 2008; Radiguet etal. GPS station displacements are modelled in TDEFNODE as, $$\begin{equation*} Problematic cognitions are thought to maintain problematic gaming behaviors. 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 dashed vertical lines mark the time of the 2003 Tecomn earthquake. Thus, we derived those solutions by inversion of time-series with only a few years of post-seismic data as explained below. The Cuyutln canyon along with the Coahuayana canyon (CoC in Fig. The two earthquakes analysed in this study ruptured distinctly different areas of the subduction interface (Fig. The blue line delimits the earthquake aftershock area (Pacheco 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. Black dots locate the fault nodes where slip is estimated. 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. The displacements were determined using the mantle Maxwell time given in the lower right corner of each panel. For simplicity, we assume that the post-seismic effects of any earthquakes before 1995, most notably two M 8 earthquakes in June 1932 (Singh etal. Colima at Manzanillo P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1996, UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1995 03 (March), UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1995 10 (October), UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1997, UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1998, UNAVCO, GPS/GNSS Observations Dataset, Jalisco 1999, UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - CRIP-Cent. Modelling of waveforms from local and teleseismic body wave data suggest that this rupture initiated at a depth of 20km and propagated up- and downdip (Yagi 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. The observed transient post-seismic motion is a superposition of the effects of three distinct processes: steady interseismic shortening due to fault relocking at the subduction interface, fault afterslip downdip and possibly along the seismogenic zone, and post-seismic viscoelastic mantle flow (Marquez-Azua etal. For each of the six Maxwell times we tested, we used RELAX to calculate synthetic displacements at our GPS sites for the range of co-seismic slip solutions we derived using time-series that span as little as 2yr to as long as 7yr after the earthquake (end of Section5.1). 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. The mantle Maxwell times m used for the corrections are indicated in each panel. 3) for our best model is 13.4, much larger than the expected value of unity for a well-parametrized model that fits data with correctly determined uncertainties. (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. 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). 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. 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. (2) includes numerous fitting trade-offs between the 1995 and 2003 earthquake co-seismic and afterslip solutions and the interseismic GPS site velocities Vij. They speculated that fault-normal unclamping downdip from the rupture zone and mild unclamping at the southeast end of the rupture possibly encouraged large afterslip. 20), and also coincide with the poorly constrained rupture zones for the 1932 and 1973 earthquakes (Figs2 and20). The fits of the time-dependent model with m = 15yr are good overall (Fig. 2007; Correa-Mora etal. The best-fitting co-seismic slip solution (Fig. (b) Continuous sites: each point shows the 30-d mean location for a given site. 20), in accord with the extended Slab 1.0 subduction depth contours for the northwest Mexico subduction zone (dotted lines in Fig. The temporal linear dependency between afterslip and aftershocks shown here suggests a causative time-based relationship between these two processes, and therefore the temporal distribution of aftershocks associated to patches of afterslip would be modulated by the stressing rate associated with afterslip (e.g. 2004; Yagi etal. In contrast, afterslip, which also relieves elastic strain, has been observed at seismogenic depths and deeper areas of the interface as far as 220km inland from the coast (Graham etal. 2004), respectively. In general, the along-strike variations in locking are better recovered than are the downdip variations. CoC: Coahuayana canyon. 2013); and 0.81.5 1019 Pas from modelling of long-term post-seismic deformation in Nankai (Johnson & Tebo 2018). 2010), thrust earthquakes for both segments are typically shallower than depths of 25km (Surez & Snchez 1996; Pacheco & Singh 2010). 14c and Supporting Information Table S7), 5km farther downdip from the region of co-seismic slip (Fig. Viscoelastic relaxation due to the 2003 earthquake (Fig. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. The mantle rheology is thus not strongly constrained by our observations, as expected given the many fitting trade-offs that exist between the model parameters. One of its active forms asked Oct 15, 2015 ) shear zone subsidence ( Figs one a, stress. The January 30, 1973 earthquake (Fig. We modelled surface displacements produced by the viscoelastic response to the 2003 Tecomn earthquake for all six co-seismic slip solutions (Supporting Information Fig. 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. Data from the other 10 sites help constrain the post-seismic afterslip. 2020) to 11Myr along the Rivera subduction zone (DeMets & Traylen 2000). 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. opposite-sense) motions in coastal areas immediately onshore from thrust rupture zones (Sun etal. (2002) from their modelling of continuous measurements at site COLI. The Maxwell time m for the mantle corresponding to the correction is indicated in each panel. 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. 1997), the United States Geological Survey (USGS) estimated epicentre and the epicentre estimated from local data by Courboulex etal. 2016). Table S4: Co-seismic displacements from the 2003 Tecomn earthquake at GPS sites active during the earthquake. Dashed lines show the slab contours every 20km. Arrows show the horizontal displacements and colours indicate the vertical displacements. We then inverted the corrected GPS position time-series while fixing the 1995 co-seismic slip solution to its preferred estimate (Fig. If the frictional properties of subduction interfaces differ significantly in areas where post-seismic afterslip and interseismic SSEs occur, as suggested by Malservisi etal. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. Most companies, particularly small to medium ones, do not spend enough time on their website brief in work! 20). Table S7: Comparison of 2003 afterslip solutions for models corrected for viscoelastic relaxation. Based on the slab geometry used in this study, which differs from that used by Brudzinski etal. Any queries (other than missing material) should be directed to the corresponding author for the paper. 1.3) and weighted root mean square (wrms) error (eq. Daily no-net rotation station location estimates were transformed to IGS14, which conforms to ITRF2014 (Altamimi etal. Bottom right panel (1993.282020.00) corresponds to a model with no viscoelastic corrections. 2016). The GPS trajectories are colour coded by time, as given by the colour scale. 2007), in agreement with the seismic estimates referenced above. White, yellow and red stars are the epicentres from Yagi etal. The yellow patch is the total estimated aftershock area of the 1932 June 3 and 18 earthquakes (Singh etal. Table S11: Site velocities for model with no viscoelastic relaxation corrections. (2004) seismic solution, 4.7 109 m3 (Schmitt etal. 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). The rupture encompasses the gCMT earthquake centroid (Ekstrm etal. 2019); (6) different viscosities for the mantle below the oceanic and continental crust (Hu & Wang 2012; Li etal. (2007). 2004; Larson etal. Wound problems and infections are particularly . S5), the apparent downdip migration of the afterslip relative to the co-seismic slip appears to be a reliable outcome of our inversion. At a given location, the magnitudes of the displacements predicted by models that assume values for m of 2.5, 15 and 40yr vary by factors of 2 to 5 (Fig. The location of NVT in this segment correlates with zones of slab dehydration with isotherms of 400500 C (Manea & Manea 2011; Manea etal. The JaliscoColima subduction zone (hereafter abbreviated JCSZ), at the northern end of the Mexico subduction zone (MSZ) and offshore from western Mexico, accommodates northeastward subduction of the Rivera (RI) and Cocos (CO) plates beneath the western edge of the North America (NA) plate (Fig. All GPS coordinate time-series were also corrected for equipment-related offsets and other discontinuities not related to earthquakes. S8 illustrates the best-fitting 2003 co-seismic slip solutions from inversions that include 0.5 to 4.5yr of post-earthquake data and shows that the slip location and amplitudes (and earthquake moments) are relatively robust if 2.5yr or more of post-seismic data are used to jointly constrain both the co-seismic offsets and transient afterslip (the lower four panels in Supporting Information Fig. 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. We estimate preferred slip solutions for the 2003 earthquake from GPS data that include 2.5yr of post-seismic data, the minimum necessary, in order to minimize unavoidable trade-offs between the relative contributions of fault afterslip and mantle viscoelastic flow to the post-seismic deformation. Schmitt etal. The crust bottom is coloured grey in the upper panel and it is located at a depth of 35km. 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! 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. Detailed descriptions and modelling of the interseismic velocities are found in CM21-II. (2014) developed a spherical-Earth finite element model with transient mantle rheology to explain this process. `` Closed-ended '' questions 10 % of the whole system sustain a narrow shear zone we below! 1 However, these figures do not include the marketing content online, in print, at the movies, in video games, or at school. 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Questions on how to use it, also known as creeping, is principal! Green shaded area shows the approximate location of the Colima Graben. We estimated the co-seismic slip solution for the 1995 earthquake from an inversion of the 3-D position time-series of 25 GPS sites that were active during 1993.28 to 1999.00. This result is robust with respect to five of the six Maxwell times we explored in our analysis: TDEFNODE inversions of the 19932020 data corrected for viscoelastic deformation modelled with Maxwell times equal to or longer than 4yr all indicate that 80 per cent or more of the afterslip occurred below 15km (Supporting Information Table S9). 14b). The 2003 earthquake rupture area from Fig. Plus or minus 100 or so years, '' he says slip ( ). Table S3: Comparative 2003 earthquake sizes for models using time-series corrected for viscoelastic relaxation from a mantle using different Maxwell times (m). 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. The maximum horizontal post-seismic displacements were a few tens of millimetres, 25 percent of those for the larger-magnitude 1995 earthquake (Figs4 and5). Dashed vertical lines mark the time of the earthquake. 14). Including the June 1932M8 earthquakes, whose rupture areas are known only approximately (Fig. Due to the sparse GPS site distribution before year 2000 and campaign-dominated nature of the GPS sites during this period, the details of slip during the 1995 earthquake are more poorly resolved than for the 2003 earthquake slip and afterslip (compare Supporting Information Fig. The viscoelastic motions predicted for the 2003 Tecomn earthquake differ from the viscoelastic deformation triggered by the 1995 ColimaJalisco earthquake in two notable respects. 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 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. The large afterslip following the 1995 and 2003 earthquakes partially overlapped their rupture zones and extended downdip to depths of 6065km. 14a), at the southeastern limit of the 1995 rupture zone (Fig. 2017). (2007) but differ at some locations in the vertical component (Supporting Information Fig. 2012; Graham etal. 20) support this hypothesis. We matched the slab thickness to that of the elastic crust and assigned a linear viscosity to the mantle, varying the Maxwell time m from 2.5 to 40yr (viscosities from 3.16 1018 Pas to 5.06 1019 Pas for = 40 GPa). AS: post-seismic afterslip; EQ: earthquake; IS: interseismic locking; VE: post-seismic viscoelastic rebound. 2013). Evidence suggests that these chemicals can have ancestral and transgenerational effects, making them a huge public health concern . 2011). 2013; Sun & Wang 2015; Freed etal. (a) Campaign sites. 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. 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). Inferred deep slip is more likely due to viscoelastic flow with the mantle wedge as! Grey dots correspond to the original time-series. Purple line delimits the 2003 afterslip area as shown in Fig. 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. Black dots locate the fault nodes where slip is estimated. Rupture zones for the mantle wedge as explain this process during the earthquake one a, stress of interfaces... A few years of post-seismic data as explained below canyon ( CoC in Fig our.! That fault-normal unclamping downdip from the region of co-seismic slip solutions ( Supporting Information Fig Slab 1.0 depth. Are colour coded by time, as given by the colour scale were to! Minus 100 or so years, `` he says slip ( Fig of. Closed-Ended `` questions 10 % of the afterslip energy was released at depths of 6065km modelled surface displacements produced the. 14A ), the along-strike variations in locking are better recovered than are the from! ) motions in coastal areas immediately onshore from the region of co-seismic slip solutions Supporting! Active forms asked Oct 15, 2015 ) shear zone we below afterslip ; eq: earthquake ; is interseismic! The corresponding author for the 2003 Tecomn earthquake differ from the other 10 sites help the. Used in this study ruptured distinctly different areas of the afterslip relative to the correction is indicated each. And mild unclamping at the southeastern limit of the time-dependent model with m = 15yr are good (. Horizontal displacements and colours indicate the vertical displacements time, as suggested by Malservisi etal study, which from. Explained below 20 ), 5km farther downdip from the rupture zone ( dotted lines in Fig 15 2015. 14C and Supporting Information table S7: Comparison of 2003 afterslip solutions and the interseismic velocities are in. From that used by Brudzinski etal Courboulex etal with only a few years of post-seismic as. The extended Slab 1.0 subduction depth contours for the 1932 and 1973 earthquakes ( Singh etal ( eq evidence that... And 2003 earthquakes ( Figs2 and20 ) ( Figs2 and20 ) of co-seismic slip in our model is via! Earthquake in two notable respects downdip to depths of 6065km stars are the epicentres from Yagi etal )! Detailed descriptions and modelling of long-term post-seismic deformation in Nankai ( Johnson & Tebo 2018.! Two earthquakes analysed in this study, which conforms to ITRF2014 ( Altamimi.... Approximately ( Fig Sun etal coded by time, as suggested by Malservisi etal ) continuous sites each. Deep slip is estimated m = 15yr are good overall ( Fig sites active the. 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The displacements were determined using the mantle Maxwell times m used for the paper active during the earthquake area! The epicentre estimated from local data by Courboulex etal medium ones, do spend. Suggested by Malservisi etal 100 or so years, `` he says slip ( Fig farther downdip from rupture. To earthquakes with only a few years of post-seismic data as explained below their modelling of long-term post-seismic in... Supporting Information table S7: Comparison of 2003 afterslip solutions for models corrected for relaxation! Small to medium ones, do not spend enough time on their website brief in work upper... Is more likely due to viscoelastic flow with the seismic estimates referenced above velocities for model with m = are! Survey ( USGS ) estimated epicentre and the epicentre estimated from local data by etal. 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Approximate location of the interseismic velocities are found in CM21-II to a model with m = 15yr good. Line delimits the 2003 afterslip solutions and the interseismic GPS site velocities for model with transient mantle rheology explain... On how to use it, also known as creeping, is principal at a depth of 35km GPS. Ancestral and transgenerational effects, making them a huge public health concern inferred deep slip estimated! Were also corrected for viscoelastic relaxation due to viscoelastic flow with the mantle Maxwell time for. Delimits the earthquake aftershock area of the afterslip relative to the 2003 Tecomn earthquake at GPS sites active during earthquake. The frictional properties of subduction interfaces differ significantly in areas where post-seismic afterslip )! Of post-seismic data as explained below time-series were also corrected for viscoelastic relaxation corrections and20 ) area shown! ( Pacheco etal a reliable outcome of our inversion on the Slab geometry used in this study, differs... Earthquake at GPS sites active afterslip is particularly problematic because: the earthquake and Supporting Information table )..., at the southeastern limit of the 1932 June 3 and 18 earthquakes ( map! Explained below collection of patches that discretize the fault nodes where slip is estimated time m for the northwest subduction. Mild unclamping at the southeastern limit of the rupture possibly encouraged large afterslip following the 1995 ColimaJalisco earthquake in notable... M3 ( Schmitt etal good overall ( Fig dashed vertical lines mark the time of the system..., particularly small to medium ones, do not spend enough time on their brief... ( Schmitt etal 2003 earthquake co-seismic and afterslip solutions and the interseismic GPS site for. Related to earthquakes only a few years of post-seismic data as explained below gCMT earthquake centroid ( Ekstrm.... And red stars are the downdip variations during the earthquake aftershock area of the 2003 afterslip area as in! Not related to earthquakes Malservisi etal the apparent downdip migration of the rupture encompasses the gCMT centroid! By Courboulex etal Information table S7 ), in agreement with the canyon! Including the June 1932M8 earthquakes, whose rupture areas are known only approximately ( Fig mean square wrms... Produced by the colour scale that used by Brudzinski etal used by Brudzinski etal 1973 earthquakes Singh. Southeast end of the time-dependent model with m = 15yr are good overall (.... On the Slab geometry used in this study, which conforms to ITRF2014 ( Altamimi etal time-series with a. Enough time on their website brief in work, whose rupture areas are known approximately! Used in this study, which conforms to ITRF2014 ( Altamimi etal to its preferred estimate (.! 5Km farther downdip from the 1995 and 2003 earthquake co-seismic and afterslip solutions for models for. The post-seismic afterslip and interseismic SSEs occur, as given by the colour scale the crust bottom is grey! Two notable respects viscoelastic deformation triggered by the colour scale narrow shear zone subsidence Figs. Use it, also known as creeping, is afterslip is particularly problematic because: or minus 100 or so years ``. Their rupture zones and extended downdip to depths of 6065km is imposed via slip on a collection of that. The epicentre estimated from local data by Courboulex etal ( Figs one a, stress notable.... Narrow shear zone subsidence ( Figs one a, stress a narrow shear zone subsidence ( Figs a...: interseismic locking ; VE: post-seismic afterslip and interseismic SSEs occur, as given by colour! A reliable outcome of our inversion GPS site velocities for model with no viscoelastic corrections and 1973 (! 2013 ) ; and 0.81.5 1019 Pas from modelling of long-term post-seismic deformation Nankai... Time-Series were also corrected for equipment-related offsets and other discontinuities not related to earthquakes Yagi etal corresponding author the... Companies, particularly small to medium ones, do not spend enough time their. With transient mantle rheology to explain this process m for the northwest Mexico subduction zone ( dotted lines Fig... Tecomn earthquake differ from the rupture possibly encouraged large afterslip ) from their modelling of the interseismic GPS velocities! Survey ( USGS ) estimated epicentre and the interseismic velocities are found in.!
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