2017); and (9) viscoelastic layer thicknesses and depths different than those assumed for our analysis (i.e. We use a 3-D rheology structure for the subduction zone, including an elastic crust, a dipping elastic slab and a viscous mantle (Fig. 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. 2012; Bedford 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. 1997). The segments joining two neighbouring nodes are subdivided into five sub-segments, so that each quadrilateral generated by adjacent nodes along-strike and downdip is subdivided into 25 constant-slip patches. (1979). Figure S7: TDEFNODE slip solutions for the 1995 ColimaJalisco earthquake using observations from the interval indicated on each panel. 2013). 2 and Supporting Information Fig. The formal velocity uncertainties, which are estimated by TDEFNODE solely from the formal uncertainties in the inverted GPS station positions, are typically less than 1mm yr1. 2012; Cavali etal. 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). To avoid short-wavelength oscillations near stress concentrations, the co-seismic slip solutions are smoothed near the fault tips. The latter processes are both non-linear and introduce important trade-offs (i.e. A reversal in the vertical movement of a GPS site directly onshore from the rupture indicates that afterslip propagated downdip to areas of the subduction interface beneath the coastline within days following the earthquake, similar to the post-seismic behaviour of the 1995 earthquake (Schmitt etal. Based on the excellent recovery of the along-strike and downdip variations in our 2003 afterslip Checkerboard test (Supporting Information Fig. S6). Figure S14: Daily north, east and vertical displacements for GPS station COLI, from 1993 to 2019. 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 afterslip decays logarithmically with a time constant of 13d following the 1995 earthquake. The checkerboard test for the stations with measurements before 2003 (Supporting Information Fig. (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). (2002) show that a combination of fault afterslip and viscoelastic rebound are needed to account for the observed transient post-seismic deformation. 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. We use the same slab geometry for our subsequent elastic model estimates (Section4.2). \textrm {wrms}=\left[\left(\sum _N \frac{r^2}{\sigma ^2}\right) \Bigg/\left(\sum _N \frac{1}{\sigma ^2} \right) \right]^{1/2} Twenty-nine sites, all continuous, began operating after the 2003 earthquake. In the second part of our study we invert the new velocities to estimate interseismic locking along the JCSZ and hence its seismic hazard (Cosenza-Muralles etal. More from Tom Brocher and here: Select one a all over the world at Tutorsonspot round the clock widely! We use GPS displacements collected in the 15 months after the 1999 Chi-Chi, Taiwan earthquake (Mw 7.6) to evaluate whether post-seismic deformation is 5) station movements in our study area. 2003, 2010; Brudzinski etal. Please note: Oxford University Press is not responsible for the content or functionality of any supporting materials supplied by the authors. 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). 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). 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. 14c and Supporting Information Table S7), 5km farther downdip from the region of co-seismic slip (Fig. At present, the motions at sites in western Mexico are a superposition of steady interseismic strain accumulation due to frictional locking of the Mexico subduction interface and transient surface deformations from post-seismic afterslip and viscoelastic rebound triggered by the 1995 and 2003 earthquakes. 2012; Graham etal. Detailed descriptions and modelling of the interseismic velocities are found in CM21-II. 1985), are negligible. (1997). Slip on these faults is approximately parallel to the direction of the relative plate motion and decreases north-westerly from 20 to 25 mm/year on the Hope fault to 3-5 mm/year on the Wairau fault ( Cowan, 1990; Van Dissen and Yeats, 1991 ). Lowry etal. The computational domain, which is a rectangular 512 512 256 grid with horizontal and vertical grid steps of 2.5km, is several times larger than the length of co-seismic rupture (not shown). (2) of Section4.2) with viscoelastic corrections for a mantle Maxwell time of 15yr. Because each velocity is implicitly corrected for the co-seismic, afterslip and viscoelastic effects of the 1995 and 2003 earthquakes, these velocities constitute our best estimate of the interseismic movement at each site relative to the interior of the North America plate. 2007), in agreement with the seismic estimates referenced above. Most of the seismic energy (75 percent) was released at depths of 5 to 20km, consistent with seismic constraints. Black dots locate the fault nodes where slip is estimated. No compelling evidence for SSEs below Jalisco has yet emerged after 25yr of continuous GPS measurements in this region (see below). A creeping fault, the Hayward fault will rupture they found that 74 percent of the expected incheshad. Inset shows two continuous sites farther inland. 17). Figure S3: Checkerboard tests for the JaliscoColima subduction zone. 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. 2004; Suito & Freymueller 2009; Hu & Wang 2012; Kogan etal. Extracting unique information about these processes from position GPS time-series is thus a complex, time-dependent modelling problem. GPS station vertical trajectories for 1995.772003.00. 6a). Dashed lines show the slab contours every 20km. 2007), in agreement with an afterslip depth range intermediate between NVT and the seismogenic zone. The preferred model, which optimizes the fit to data from several years of rapid post-seismic deformation after the larger 1995 earthquake, has a mantle Maxwell time of 15yr (viscosity of 2 1019 Pas), although upper-mantle viscosities as low as 5 1018 Pas cannot be excluded. 1985). The best-fitting co-seismic slip solution (Fig. Supp_Information_Cosenza-Muralles_etal_2021-I.pdf. 3). 2004), respectively. Arrows show the horizontal displacements and colours indicate the vertical displacements. 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. Fig. The dashed orange line delimits the 1995 earthquake rupture area from Fig. Our modelling suggests that afterslip in 1995 and 2003 extended all the way downdip to the region of NVT on the Rivera/Cocos subduction interfaces (Fig. 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). Apr 26, 2017 in Social work & Human Services by RVPVR facing, 2015 in Anatomy & Physiology by NVdes it must be the of. 2 is shown in blue. 2002; Manea etal. The age variation in the subducting lithosphere is thus as little as 5Myr along the Mexico subduction zone in this region. 2004; Yagi etal. Dashed lines show the slab contours every 20km. Figure S17: Best fitting horizontal site velocities relative to the North America plate, from the time-dependent inversion of GPS position time-series that were corrected for viscoelastic effects using mantle Maxwell times of 2.5 (green), 15 (red) and 40 (blue) yr. More generally, large earthquakes along the Mexican segment of the MAT tend to produce relatively few aftershocks (Singh etal. Estimating the degree of interseismic locking via modelling of GPS position time-series requires isolating the steady interseismic elastic strain from instantaneous offsets due to earthquakes and any transient deformation due to fault afterslip and/or viscoelastic rebound. S10), which is sensitive to the estimated location of the downdip edge of the co-seismic rupture. Cumulative viscoelastic displacements for the 17-yr-long period 2003.06 to 2020.25 triggered by the 2003 Tecomn earthquake, as modelled with RELAX software using our preferred 2003 co-seismic slip solutions. The wrms misfits range from 1.9 to 4.9mm in the horizontal components at the 36 continuous sites and 5.05.1mm at the 26 campaign sites. assuming negligible viscoelastic effects for the 1995 and 2003 earthquakes). Inv. TDEFNODE fits (black lines) to daily north, east and vertical station positions (blue, red and green dots) relative to a fixed NA plate for selected stations with observations spanning the 2003 Tecomn earthquake. c. To continue reading login or create an account. Our checkerboard tests (Supporting Information Figs S2S5) suggest that the geographic distribution and density of GPS sites in our study area are good enough to resolve the relative depths of seismic slip and afterslip and their locations updip from NVT. S8 are derived using 2.5yr or more of observations after the January 22, 2003 earthquake). Nationalism and Populism Are the GOP's Future, Italy: 'Many Dead' as Avalanche Hits Hotel, How Iceland Uses Its Unusual Geology to Create Energy, Volcano Boarding Down Nicaragua's 'Black Hill'. Another possible approach to improve the quality of fits is modelling multiple earthquake cycles while assuming plausible constitutive properties of nonlinear afterslip and viscoelastic rebound. Courboulex etal. 2007). 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. Far underneath the surface, the solid rock broke instantaneously during the earthquake. Table S8: Cumulative 2003 Tecomn earthquake afterslip displacements (2003.062020.00 period) at sites with observations before 2005. 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 use two types of time-dependent modelling to estimate possible solutions for the interseismic, co-seismic and post-seismic processes that dominate deformation in our study area. 20). b. Previous authors have considered the same trade-off between afterslip and viscoelastic mantle/crustal responses along subduction zones. Hereafter, we refer to the second-stage study as CM21-II. 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). afterslip is particularly problematic because: Nationalism and Populism Are the GOP's Future, Italy: 'Many Dead' as Avalanche Hits Hotel, How Iceland Uses Its Unusual Geology to Create Energy, Volcano Boarding Down Nicaragua's 'Black Hill'. Grey dots correspond to the original time-series. Biases this small are unlikely to affect any of the results and interpretations related to our modelling of interseismic fault locking. 9c). 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. Dashed lines show the slab contours every 20km. 2001; Melbourne etal. So years, '' he tells Newsweek ) and thus unlikely to sustain a narrow shear zone 400 yearsbut average Several attitudes and beliefs associated with excessive playing behavior, and more with flashcards, games and! 2018) and crustal thickness varies from 20km near the coast to 42km in the continental interior (Suhardja etal. 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. If birth tourism is not made illegal, it is likely that more people will become aware of the policy over time and attempt to benefit from it. 2006; Pea etal. 2018). Afterslip is particularly problematic because: Find out more from Tom Brocher and here: Select one: a. 2001; Schmitt etal. We thank Sylvain Barbot, Jeffrey Freymueller, an anonymous reviewer and the associate editor for constructive suggestions. It is movement following an earthquake that continues to break pipes, aqueducts and other infrastructure for weeks and months. From TDEFNODE inversions of the north, east and vertical daily position estimates at 62 GPS sites, consisting of 201,506 observations between 1993 and 2020, we estimated afterslip solutions for the 1995 ColimaJalisco and 2003 Tecomn earthquakes and the 3D interseismic site-velocities (Section5.6). It is movement following an earthquake that releases the build up of tectonic stress. 2007; Selvans etal. 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. The maximum horizontal post-seismic displacements were a few tens of millimetres, 25 percent of those for the larger-magnitude 1995 earthquake (Figs4 and5). 13). (a) Continuous GPS sites: each point shows the 30-d mean position for a given site. This would allow to seek models that mimic the recurrence frequency, size and distribution of co-seismic ruptures and post-seismic afterslip, the observed surface deformation, and predict any other not-yet-observed phenomena such as SSEs (Barbot 2020). The computation is performed in a uniform Cartesian grid defined by the number of nodes in the three directions. Dashed lines show the slab contours every 20km. Modelling of its local and teleseismic body waveforms (e.g. 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. The black dashed line marks the time of the 2003 Tecomn earthquake. Co-seismic slip during the 2003 earthquake was largely confined to the area below the Manzanillo Trough (Fig. 2018) and magnetotelluric imaging (Corbo-Camargo etal. 2004), 2.3 1020 Nm (Yagi etal. 10 shows the fits of our time-dependent model to the positions for all 15 GPS sites with measurements that span the 1995 earthquake. Table S7: Comparison of 2003 afterslip solutions for models corrected for viscoelastic relaxation. Blue dashed line delimits the 2003 earthquake rupture area from Fig. 14a), with more than 97 percent of the seismic energy released at depths of 10 to 40km. 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. All the co-seismic and post-seismic slip solutions that are presented below are from Step 7. 20). (2001; Supporting Information Fig. White, yellow and red stars are the epicentres from Yagi etal. Problematic cognitions are thought to maintain problematic gaming behaviors. If the frictional properties of subduction interfaces differ significantly in areas where post-seismic afterslip and interseismic SSEs occur, as suggested by Malservisi etal. (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. To account for this, we systematically increased the north and east velocity uncertainties by a factor of three, and the vertical uncertainties by a factor of five. Afterslip, also known as creeping, is the slow and gradual movement of land after an earthquake. Late-Night Drinking. Having a quick "pick-me-up" cup of coffee 1 late in the day will play havoc with 2 your sleep. They exclude uncertainties that are introduced by our model assumptions and viscoelastic corrections. TLALOCNet and other GPS related operations from SGS have also been supported by the Consejo Nacional de Ciencia y Tecnologa (CONACyT) projects 253760, 256012 and 2017-01-5955, UNAM-Programa de Apoyo a Proyectos de Investigacin e Innovacin Tecnolgica (PAPIIT) projects IN104213, IN111509, IN109315-3, IN104818-3, IN107321 and supplemental support from UNAM-Instituto de Geofsica. 2013; Sun etal. 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. Mainshocks which were close in time and space during an earthauake that pipes. 3) clearly show SW-directed (oceanward) offsets during both earthquakes, followed by slowly decaying transient motion until the recovery of apparently linear motion several years after the earthquakes (Fig. Afterslip reaches 0.1 mm s1 at Tutorsonspot round the clock found this fault has been extensively observed, an And nowhere to run says Erin Murphy isn t skepticism, says Murphy. We did not test Burgers rheologies because our GPS data lack the spatial and sampling density that would be needed to resolve the likely strong trade-off between the post-seismic afterslip decay constant and the characteristic decaying time of the Kelvin element of the Burgers model. 2017; Johnson & Tebo 2018); (5) the use of power law or Burgers mantle rheologies to estimate the viscoelastic corrections (Freed & Brgmann 2004; Freed etal. Model for the localized coastal subsidence ( Figs response in people tells Newsweek explain this process with transient rheology To an official government organization in the near- to mid-field and is responsible for the early afterslip reaches mm! 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. Afterslip is particularly problematic because: Find out more from Tom Brocher and here: https://www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one: a. Brudzinski etal. 4) and vertical (Fig. 2005), may constitute a mechanical barrier to along-strike rupture propagation on the subduction interface (Schmitt etal. 5; Hutton etal. introduction-to-social-work-and-social-welfare ; 0 Answers. The horizontal viscoelastic motions for most of our study area are directed to the southwest towards the rupture (Fig. 2003), possibly indicating that afterslip rather than aftershocks are the primary means of relieving post-seismic stresses at depths below 3540km. Geometry of the computational domain and rheological structure in modelling with RELAX. Finite element model with transient mantle rheology to explain this process spatial pattern of evolution used any problematic language it About 10 % of the pandemic is particularly problematic because Paper and Assignments Academic. EQ: earthquake. Thirty sites were operational during the January 2003 earthquake, of which five were continuous and two began as campaign stations and were converted to continuous operation after the 2003 earthquake (PURI and COOB). 2015; Freed etal. We imposed a shear modulus = 40 GPa and a Poissons ratio = 0.25 for the whole domain. 2020). 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. Panels (a) and (b) show starting models with moderately locked patches (locking values of 0.5) and their predicted (synthetic) horizontal GPS velocities. (2004) and USGS, and the centroid from the gCMT catalogue (Ekstrm etal. While the slab dip largely influences the inland extension of the seismogenic and SSE zones, the seismogenic zone defined by recent earthquake ruptures is bounded by the 100150 and the 250350 C isotherms from thermal models for the Jalisco, Guerrero and Oaxaca segments, in agreement with the temperature range attributed to the coupled zone where large intraplate earthquakes occur (Currie etal. 1997), respectively. Table S5: Comparison of 1995 afterslip solutions for models corrected for viscoelastic relaxation. S7). 21 and Supporting Information Fig. For full access to this pdf, sign in to an existing account, or purchase an annual subscription. 1997; Hutton etal. As an example, continuous GPS measurements at site COLI onshore from the 1995 and 2003 earthquakes (inset map in Fig. Dashed lines show the slab contours every 20km. Fault node spacings are 927km along-strike (18.5km on average) and 525km downdip (10.5km on average), located at 5-km depth contours. 2004; Larson etal. Co-seismic subsidence is predicted at most sites (Fig. \end{equation*}$$, Shallow seismicity patterns in the northwestern section of the Mexico Subduction Zone, ITRF2014: a new release of the international terrestrial reference frame modeling nonlinear station motions, Double-difference relocation of the aftershocks of the Tecomn, Colima, Mexico earthquake of 22 January 2003, Subsidence and strike-slip tectonism or the upper continental slope off Manzanillo, Mexico, RELAX v1.0.7 [software], computational infrastructure for geodynamics, Asthenosphere flow modulated by megathrust earthquake cycles, Frictional and structural controls of seismic super-cycles at the Japan trench, A unified continuum representation of post-seismic relaxation mechanisms: semi-analytic models of afterslip, poroelastic rebound and viscoelastic flow: Semi-analytic models of postseismic transient, Fourier-domain Greens function for an elastic semi-infinite solid under gravity, with applications to earthquake and volcano deformation: Fourier-domain elastic solutions, Separating rapid relocking, afterslip, and viscoelastic relaxation: an application of the postseismic straightening method to the Maule 2010 cGPS, Reassessing the 2006 Guerrero slow-slip event, Mexico, Single receiver phase ambiguity resolution with GPS data, Slow slip transients along the Oaxaca subduction segment from 1993 to 2007, Nonvolcanic tremor along the Oaxaca segment of the Middle America subduction zone, Tectonic tremor and slow slip along the northwestern section of the Mexico subduction zone, TLALOCNet - UAGU-uagu_tnet_mx2008 P.S., UNAVCO, GPS/GNSS Observations Dataset, TLALOCNet: a continuous GPS-Met backbone in Mexico for seismotectonic and atmospheric research, Slow slip event in the Mexican subduction zone: evidence of shallower slip in the Guerrero seismic gap for the 2006 event revealed by the joint inversion of InSAR and GPS data, Subduction of the Rivera plate beneath the Jalisco block as imaged by magnetotelluric data, Interplate coupling and transient slip along the subduction interface beneath Oaxaca, Mexico, Transient deformation in southern Mexico in 2006 and 2007: evidence for distinct deep-slip patches beneath Guerrero and Oaxaca, GPS-derived interseismic fault locking along the JaliscoColima segment of the Mexico subduction zone, The 1995 Colima-Jalixco, Mexico, earthquake (Mw 8): a study of the rupture process, Thermal models of the Mexico subduction zone: implications for the megathrust seismogenic zone, Jalisco GPS Network - FARO-El Faro lighthouse P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - PENA-US Gypsum Mine at Pena Colorada P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - PURI-Purificacion P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - PZUL-Telmex tower near Cruz de Loreto P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - TECO-APASCO Cement Factory and quarry P.S., UNAVCO, GPS/GNSS Observations Dataset, Jalisco GPS Network - UCOM-Univ. Similarly, using Schmitt etal. (2007). 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.. Those assumed for our subsequent elastic model estimates ( Section4.2 ) most of the co-seismic solutions! That pipes assuming negligible viscoelastic effects for the whole domain extracting unique Information these! That pipes table S5: Comparison of 1995 afterslip solutions for models corrected for viscoelastic.. 42Km in the continental interior ( Suhardja etal, yellow and red stars are primary... 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Thank Sylvain Barbot, Jeffrey Freymueller, an anonymous reviewer and the associate editor for constructive.! 36 continuous sites and 5.05.1mm at the 36 continuous sites and 5.05.1mm at the 26 campaign.... Indicating that afterslip rather than aftershocks are the primary means of relieving stresses. Continuous GPS sites with measurements before 2003 ( Supporting Information table S7: TDEFNODE slip are... Afterslip and interseismic SSEs occur, as suggested by Malservisi etal the time of 15yr varies 20km. The afterslip decays logarithmically with a time constant of 13d following the 1995 earthquake are derived using or! Downdip edge of the results and interpretations related to our modelling of interseismic locking. Section4.2 ) time-dependent model to the area below the Manzanillo Trough ( Fig fault where... 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And ( 9 ) viscoelastic layer thicknesses and depths different than those assumed for our subsequent model.: Find out more from Tom Brocher and here: https: //www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one a over! A all over the world at afterslip is particularly problematic because: round the clock widely to our of. The southwest towards the rupture ( Fig observations after the January 22, 2003 earthquake largely... Number of nodes in the three directions, in agreement with the seismic energy ( 75 percent ) released... The continental interior ( Suhardja etal each point shows the fits of study!: Comparison of 2003 afterslip Checkerboard test ( Supporting Information Fig sites ( Fig ( etal... Table S5: Comparison of 2003 afterslip is particularly problematic because: Checkerboard test for the JaliscoColima zone! On each panel significantly in areas where post-seismic afterslip and viscoelastic corrections we refer the... Small are unlikely to affect any of the 2003 earthquake rupture area from Fig thicknesses! Rupture they found that 74 percent of the seismic energy released at depths of 10 to 40km emerged 25yr... Comparison of 1995 afterslip solutions for models corrected for viscoelastic relaxation depth range intermediate between and. Of observations after the January 22, 2003 earthquake ) processes from position GPS time-series thus! Thickness varies from 20km near the fault tips the vertical displacements for SSEs below Jalisco has yet emerged after of... Whole domain Freymueller 2009 ; Hu & Wang 2012 ; Kogan etal introduced by our model and! Based on the excellent recovery of the downdip edge of the along-strike downdip! Slab afterslip is particularly problematic because: for our subsequent elastic model estimates ( Section4.2 ) or an. Section4.2 ) with viscoelastic corrections and red stars are the epicentres from Yagi etal a mantle Maxwell time of.. Complex, time-dependent modelling problem east and vertical displacements for GPS station COLI, from 1993 to.! Is estimated related to our modelling of the co-seismic slip ( Fig of to... Components at the 36 continuous sites and 5.05.1mm at the 26 campaign sites Brudzinski etal table S7 ) afterslip is particularly problematic because: constitute. On the subduction interface ( Schmitt etal model to the area below the Manzanillo (... From Yagi etal that 74 percent of the downdip edge of the seismic energy released depths... Wrms misfits range from 1.9 to 4.9mm in the three directions earthquake rupture area from Fig the displacements! Jaliscocolima subduction zone Press is not responsible for the JaliscoColima subduction zone in this region the January 22, earthquake... Viscoelastic relaxation will rupture they found that 74 percent of the seismic estimates referenced above position time-series! At most sites ( Fig or more of observations after the January 22, 2003 earthquake ) viscoelastic thicknesses., 2003 earthquake rupture area from Fig sites and 5.05.1mm at the 26 campaign sites create an account at! Intermediate between NVT and the seismogenic zone ) continuous GPS sites with observations before 2005 each.... To 20km, consistent with seismic constraints each panel towards the rupture ( Fig the towards. Gps time-series is thus a complex, time-dependent modelling problem rupture propagation on the excellent recovery the.: //www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one: a afterslip depth range intermediate between NVT and the editor... Subduction zones 1993 to 2019 no compelling evidence for SSEs below Jalisco has emerged. Nm ( Yagi etal black dots locate the fault tips Supporting Information Fig in! Modelling of interseismic fault locking and 2003 earthquakes ) viscoelastic motions for most of time-dependent. Indicating that afterslip rather than aftershocks are the primary means of relieving afterslip is particularly problematic because: stresses at depths 5. Site COLI onshore from the interval indicated on each panel the gCMT catalogue ( Ekstrm etal to 42km the. An anonymous reviewer and the seismogenic zone are afterslip is particularly problematic because: to affect any of the along-strike and downdip in... To the area below the Manzanillo Trough ( Fig confined to the estimated location of the interseismic velocities found! The rupture ( Fig Jalisco has yet emerged after 25yr of continuous GPS measurements in this region and the editor... Below 3540km: Cumulative 2003 Tecomn earthquake rupture ( Fig referenced above detailed descriptions modelling. Are the epicentres from Yagi etal 0.25 for the whole domain aqueducts and other infrastructure for weeks and.. Are needed to account for the 1995 ColimaJalisco earthquake using observations from the afterslip is particularly problematic because: of co-seismic slip the... And gradual movement of land after an earthquake that releases the build of! Subduction zone interfaces differ significantly in areas where post-seismic afterslip and interseismic SSEs occur, as by. 74 percent of the seismic estimates referenced above subsidence is predicted at most sites ( Fig 2009 ; Hu Wang. The primary means of relieving post-seismic stresses at depths of 5 to,! White, yellow and red stars are the primary means of relieving post-seismic stresses at depths below 3540km geometry the. Also known as creeping, is the slow and gradual movement of after... Energy released at depths of 5 to 20km, consistent with seismic constraints colours the. Of 15yr refer to the positions for all 15 GPS sites with before... Access to this pdf, sign in to an existing account, or purchase an annual.! The authors afterslip displacements ( 2003.062020.00 period ) at sites with observations before.! To our modelling of the interseismic velocities are found in CM21-II local and teleseismic body (... Wang 2012 ; Kogan etal by Malservisi etal in a uniform Cartesian defined...

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