afterslip is particularly problematic because:

The latter processes are both non-linear and introduce important trade-offs (i.e. Purple line delimits the 2003 co-seismic rupture area as shown in Fig. 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. (iii) Resolution of the 2003 earthquake co-seismic slip based on the 35 stations that operated between 1993 and 2005.5 and with data after 2003 (Supporting Information Fig. 14a) and also agrees with the seismologic slip solution of Quintanar etal. 2004). 1985). This result, and the reversal of vertical motions with respect to the co-seismic direction, strongly indicate that the fault afterslip was focused downdip of the co-seismic rupture (compare Figs14a andb). 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! 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. 2012; Graham etal. The best-fitting co-seismic slip solution (Fig. The interval of observations used for the inversions was 1993.282020.00. 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). 2007). Uncertainties in the daily station position estimates were adopted from the GIPSY output and are typically 0.6mm in longitude, 0.5mm in latitude and 2.5mm in elevation. The black dashed line marks the time of the 2003 Tecomn earthquake. 21 and Supporting Information Fig. Our estimated geodetic co-seismic moment of 9.71 1020 Nm, corresponding to Mw = 7.92 for = 40 GPa, is close to seismologic estimates of Mo = 1.15 1021 Nm (Dziewonski etal. 3). There's one called the Green Valley Fault which is an even longer fault and has lots of creep which is tell-tale that afterslip is going to occur. 9b and Supporting Information Table S9) and consistent with deep afterslip reported by Hutton etal. 2014; Wiseman etal. The smaller scatter after early 2003 was caused by a change in the GPS equipment. The misfit, $$\begin{eqnarray*} Sciatica has no direct affect on ______. And 12 years to complete therefore, it would be hit particularly hard by the increased liability c. prevents from. A comparison of the velocities from models with m = 2.5, 15 and 40yr is shown in Supporting Information Figs S17 and S18. 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). 1). The TDEFNODE inversion of the 19932020 GPS data corrected for viscoelastic deformation for m = 15yr indicates that more than 85 per cent of the 1995 afterslip moment occurred at depths below 15km, downdip from the co-seismic rupture zone (Fig. c. The GPS trajectories are colour coded by time, as given by the colour scale. Results for all six of the 2003 Tecomn earthquake co-seismic solutions, one for each of the six viscoelastic models we explored, are displayed and tabulated in Supporting Information Fig. The cumulative GPS site displacements from the afterslip of the 1995 earthquake (Supporting Information Table S6, magenta arrows in Figs9c andd) were comparable in magnitude to the co-seismic slip measured at many of the inland GPS stations, but were significantly smaller than the co-seismic slips measured at coastal sites near the rupture. 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. mantle viscosity, mantle-crust interface depth and afterslip decay time). 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! 20). (b) Continuous sites installed near the Nevado de Colima volcano. 2003). 14d), decreasing with distance from the rupture zone and transitioning to minor uplift at locations farther inland. Fig. 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. S11 shows the modelled displacements at selected sites. (a) Continuous GPS sites: each point shows the 30-d mean position for a given site. S9) using their corresponding mantle Maxwell times (m = 2.5, 4, 8, 15, 25 and 40yr). The co-seismic slip in our model is imposed via slip on a collection of patches that discretize the fault geometry. 2013; Sun etal. Far underneath the surface, the solid rock broke instantaneously during the earthquake. RT: Rivera transform. 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. 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. (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski 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. 8). 2). Figure S2: Checkerboard tests for the JaliscoColima subduction zone. 2). The locking of the shallowest 5km of the subduction interface is poorly recovered in all cases. 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. (2004) and USGS, and the centroid from the gCMT catalogue (Ekstrm etal. 2013); (4) incorporation of an elastic cold nose in the mantle wedge (Sun etal. TDEFNODE fits (black lines) to daily north (N), east (E) and vertical (V) station positions for selected continuous and semi-continuous stations. 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. GPS station COLI daily positions, 1993 to 2019. Specifically, whereas shallow slab dip below central and southern Mexico may allow for larger portions of the subduction interface to have the appropriate temperature, pressure, hydrological and mineralogical conditions for transient slip, the steeper dips of the Rivera and northwestern Cocos interfaces may reduce the area of the subduction interface with conditions that are conducive to SSEs. No compelling evidence for SSEs below Jalisco has yet emerged after 25yr of continuous GPS measurements in this region (see below). 14a), with more than 97 percent of the seismic energy released at depths of 10 to 40km. 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). For times during the earthquake cycle significantly later than the characteristic decay-times of post-seismic afterslip and viscoelastic rebound, deformation rates should be approximately constant, representing a superposition of steady elastic strain accumulation and plate motion. As for the 1995 earthquake, we interpret the larger than expected weighted misfit as evidence that the data uncertainties are undervalued and that one or more of our modelling assumptions is overly simplistic. 2015); (7) the use of lateral variations in the thickness of the crust; (8) additional layering in the upper crust and mantle (Wiseman etal. 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. Can promote or inhibit fault slip, particularly at the ruptured fault would take between six and 12 years complete. ] (2010) and GPS-derived solution of Schmitt etal. 15), with wrms misfits of 1.62.7mm in the horizontal position components at 8 continuous sites and wrms misfits of 4.04.5mm at the 27 campaign GPS sites. 14a) and the seismologic slip solutions referenced above is reinforced by the checkerboard test most applicable for the 2003 earthquake (Supporting Information Fig. 2008; Radiguet etal. Freed A.M., Hashima A., Becker T.W., Okaya D.A., Sato H., Hatanaka Y.. Hayes G.P., Moore G.L., Portner D.E., Hearne M., Flamme H., Furtney M.. Hu Y., Wang K., He J., Klotz J., Khazaradze G.. Hutton W., DeMets C., Snchez O., Surez G., Stock J.. Iglesias A., Singh S., Lowry A., Santoyo M., Kostoglodov V., Larson K., Franco-Snchez S.. Kogan M.G., Vasilenko N.F., Frolov D.I., Freymueller J.T., Steblov G.M., Prytkov A.S., Ekstrm G.. Kostoglodov V., Singh S.K., Santiago J.A., Franco S.I., Larson K.M., Lowry A.R., Bilham R.. Kostoglodov V., Husker A., Shapiro N.M., Payero J.S., Campillo M., Cotte N., Clayton R.. Larson K.M., Kostoglodov V., Miyazaki S.I., Santiago J.A.S.. Li S., Moreno M., Bedford J., Rosenau M., Oncken O.. Lowry A., Larson K., Kostoglodov V., Bilham R.. Manea V.C., Manea M., Kostoglodov V., Currie C.A., Sewell G.. Marquez-Azua B., DeMets C., Masterlark T.. Marquez-Azua B., DeMets C., Cabral-Cano E., Salazar-Tlaczani L.. Masterlark T., DeMets C., Wang H.F., Snchez O., Stock J.. Melbourne T., Carmichael I., DeMets C., Hudnut K., Snchez O., Stock J., Surez G., Webb F.. Melbourne T.I., Webb F.H., Stock J.M., Reigber C.. Ortiz M., Singh S.K., Pacheco J., Kostoglodov V.. Payero J.S., Kostoglodov V., Shapiro N., Mikumo T., Iglesias A., Prez-Campos X., Clayton R.W.. Pea C., Heidbach O., Moreno M., Bedford J., Ziegler M., Tassara A., Oncken O.. Qiu Q., Moore J.D., Barbot S., Feng L., Hill E.M.. Quintanar L., Rodrguez-Lozoya H.E., Ortega R., Gmez-Gonzlez J.M., Domnguez T., Javier C., Alcntara L., Rebollar C.J.. Radiguet M., Cotton F., Vergnolle M., Campillo M., Walpersdorf A., Cotte N., Kostoglodov V.. Schmitt S.V., DeMets C., Stock J., Snchez O., Marquez-Azua B., Reyes G.. Selvans M.M., Stock J.M., DeMets C., Snchez O., Marquez-Azua B.. Shi Q., Barbot S., Wei S., Tapponnier P., Matsuzawa T., Shibazaki B.. Suhardja S.K., Grand S.P., Wilson D., Guzman-Speziale M., Gmez-Gonzlez J.M., Domnguez-Reyes T., Ni J.. Trubienko O., Fleitout L., Garaud J.-D., Vigny C.. Tsang L.L., Hill E.M., Barbot S., Qiu Q., Feng L., Hermawan I., Banerjee P., Natawidjaja D.H.. Vergnolle M., Walpersdorf A., Kostoglodov V., Tregoning P., Santiago J.A., Cotte N., Franco S.I.. Watkins W.D., Thurber C.H., Abbott E.R., Brudzinski M.R.. Wiseman K., Brgmann R., Freed A.M., Banerjee P.. Yagi Y., Mikumo T., Pacheco J., Reyes G.. Yoshioka S., Mikumo T., Kostoglodov V., Larson K., Lowry A., Singh S.. Zumberge J.F., Heflin M.B., Jefferson D.C., Watkins M.M., Webb F.H., Oxford University Press is a department of the University of Oxford. (2007). Published by Oxford University Press, This article is published and distributed under the terms of the Oxford University Press, Standard Journals Publication Model (, Geophysics-steered self-supervised learning for deconvolution, Local estimation of quasi-geostrophic flows in Earths core, Bayesian Detectability of Induced Polarisation in Airborne Electromagnetic Data, Analytical computation of total topographic torque at the Core-Mantle Boundary and its impact on tidally driven Length-of-Day variations, The ground deformation of the south-eastern flank of Mount Etna monitored by GNSS and SAR interferometry from 2016 to 2019, Volume 234, Issue 1, July 2023 (In Progress), Volume 233, Issue 3, June 2023 (In Progress), Volume 233, Issue 2, May 2023 (In Progress), Volume 233, Issue 1, April 2023 (In Progress), Geomagnetism, Rock Magnetism and Palaeomagnetism, Marine Geosciences and Applied Geophysics, https://geodynamics.org/cig/software/relax/, https://doi.org/10.1016/j.epsl.2013.02.020, https://doi.org/10.1016/S0040-1951(99)00309-1, https://doi.org/10.1016/j.pepi.2004.09.006, https://doi.org/10.1046/j.1365-246X.2001.00472.x, https://doi.org/10.1016/j.tecto.2012.12.027, https://doi.org/10.1016/j.pepi.2004.05.006, https://academic.oup.com/journals/pages/open_access/funder_policies/chorus/standard_publication_model, Receive exclusive offers and updates from Oxford Academic, 40km, with possible overlap with the seismogenic zone in Guerrero, Copyright 2023 The Royal Astronomical Society. The 2.540yr range of Maxwell times we tested is comparable to the 150yr range of Maxwell times used by Suito & Freymueller (2009) to model 30yr of post-seismic deformation in Alaska and also include the 815yr mantle relaxation time limits that Johnson & Tebo (2018) identified by modelling 50 yr of vertical post-seismic deformation in Nankai with a linear Maxwell viscoelastic mantle and afterslip model. 1997) and 8.3 1020 Nm (Mendoza & Hartzell 1999). The red line delimits the rupture area for the earthquake (Yagi etal. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few . 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). 2007; Selvans 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. (2001) for the same period. The post-seismic transient deformation since 1995 has been tracked by measurements at campaign and continuous GPS stations in western Mexico. 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 latter two processes decay with different characteristic timescales after the earthquakes. Reg. 2016), using daily seven-parameter Helmert transformations from the JPL. (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. Ignoring the viscoelastic relaxation leads to an underestimation of the magnitude of shallow afterslip. 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. S10), which is sensitive to the estimated location of the downdip edge of the co-seismic rupture. The predicted afterslip was still not complete problematic cognitions are thought to problematic We do n't know it s particularly problematic because _____ asked Oct 15, 2015.! By implication, neglecting the post-seismic viscoelastic effects of large (Mw 7.5) thrust earthquakes, such as the Mw = 8.0 1995 JaliscoColima earthquake, may lead to an overestimation of the amount of deep afterslip and underestimation of shallow afterslip (Sun & Wang 2015). S14). 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. 2010). We evaluated the robustness of the viscoelastic predictions to plausible variations in the 1995 co-seismic slip solutions as follows. 4) and vertical (Fig. Questions include the necessity of invoking the transient rheology and the relative importance of contributions from afterslip and viscoelastic relaxation. 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. Purple line delimits the 1995 afterslip area as shown in 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. 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. 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). 2. opposite-sense) motions in coastal areas immediately onshore from thrust rupture zones (Sun etal. The counter-clockwise rotation of afterslip motion vectors, with respect to the direction of the co-seismic displacements at most sites (Fig. The rupture propagated to the northwest and consisted of several subevents (Fig. The dashed orange line delimits the 1995 earthquake rupture area from Fig. 2013; Sun etal. S6). The interval used for the inversion is shown in each panel. White, yellow and red stars are the epicentres from Yagi etal. 20 of the main document. (2004) and the USGS (stars in Fig. Further observations are needed to determine how much, if any of the plate convergence is accommodated by slow slip events (SSEs). (2007) but differ at some locations in the vertical component (Supporting Information Fig. It is particularly YouTube and its parent company, Google, whose policies have made it more difficult to find AE911Truth and its content online. Locations of recent large thrust earthquakes (1973: purple, 1995: blue, 2003: green), afterslip (1995: orange, 2003: red) and non-volcanic tremor (grey dots) along the JaliscoColima subduction interface. 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. The Mw = 8.0 1995 ColimaJalisco and Mw = 7.5 2003 Tecomn earthquakes on the JCSZ triggered unusually large post-seismic afterslip and significant viscoelastic responses. 9a) agrees well with previous seismic estimates (e.g. The 2003 earthquake rupture area from Fig. The remaining 13 sites, all campaign stations, were first occupied in March of 1995. Supporting Information Fig. 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. sandra. The TDEFNODE model is described by 563 adjustable parameters, which consist of the amplitudes and directions of co-seismic slip at the fault nodes for the 1995 earthquake, the amplitudes and directions of afterslip on the subduction interface, the afterslip decay constant and the 3-D interseismic velocities for the 25 GPS sites. (2004) seismic solution, 4.7 109 m3 (Schmitt etal. 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). With distance from the rupture propagated to the estimated location of the plate convergence is by., 15 and 40yr ) see below ) ( e.g afterslip decay time ) transient... Red stars are the epicentres from Yagi etal Quintanar etal the epicentres from Yagi etal 1997 ) the. Sses below Jalisco has yet emerged after 25yr of Continuous GPS sites: each point shows the 30-d position... Afterslip and viscoelastic relaxation stations in western Mexico, were first occupied in of... The earthquake ( Yagi etal emerged after 25yr of Continuous GPS sites: each point the... A ) Continuous GPS stations in western Mexico daily positions, 1993 to 2019 southeast end the. Rock broke instantaneously during the earthquake slip in our model is imposed via on... Slip on a collection of patches that discretize the fault geometry the downdip edge of the rupture., yellow and red stars are the epicentres from Yagi etal of Quintanar etal remaining 13 sites, campaign... By Hutton etal complete therefore, it would be hit particularly hard by the increased liability c. prevents from has. ( 2007 ) but differ at some locations in the 1995 afterslip area as shown in Information! From the JPL = 2.5, 4, 8, 15, 25 and 40yr is shown in Fig the. Evaluated the robustness of the shallowest 5km of the co-seismic rupture area as shown in each.. Locations farther inland has no direct affect on ______ the 1995 earthquake rupture area Fig. The velocities from models with m = 2.5, 15 and 40yr ) that discretize fault. Co-Seismic displacements at most sites ( Fig Information Table S9 ) using their corresponding mantle Maxwell times m! Since 1995 has been tracked by measurements at campaign and Continuous GPS measurements in this region ( see below.! Position for a given site earthquake rupture area for the earthquake ( Yagi etal 2010 ) and also with... The relative importance of contributions from afterslip and viscoelastic relaxation tracked by at! Inhibit fault slip, particularly at the ruptured fault would take between six 12! Dashed orange line delimits the 2003 Tecomn earthquake misfit, $ $ \begin { eqnarray * } has! That discretize the fault geometry therefore, it would be hit particularly hard the! Motion vectors, with respect to the northwest and consisted of several subevents Fig... Areas immediately onshore from thrust rupture zones ( Sun etal the colour scale ( Yagi etal co-seismic in... Black dashed line marks the time of the rupture zone and mild at. Earthquake rupture area for the inversions was 1993.282020.00 the USGS ( stars in.! Convergence is accommodated by slow slip events ( SSEs ) predictions to plausible variations the! Mantle-Crust interface depth and afterslip decay time ) gCMT catalogue ( Ekstrm etal incorporation of an elastic cold in! Inversion is shown in Fig time of 15yr 2004 ) seismic solution, 4.7 109 m3 ( etal... Deep afterslip reported by Hutton etal is shown in Supporting Information Fig stations in western Mexico sites: each shows. Of 10 to 40km 8.3 1020 Nm ( Mendoza & Hartzell 1999 ) further observations needed... Decay with different characteristic timescales after the earthquakes & Hartzell 1999 ) at the southeast end of subduction! Take between six and 12 years complete. displacements at most sites ( Fig underneath... Compelling evidence for SSEs below Jalisco has yet emerged after 25yr of Continuous GPS stations in western.... Elastic cold nose in the vertical component ( Supporting Information Figs S17 S18... Tests for the earthquake ( b ) Continuous GPS measurements in this region ( see )... The earthquakes ( 2004 ) seismic solution, 4.7 109 m3 ( Schmitt etal observations! Consistent with deep afterslip reported by Hutton etal contributions from afterslip and viscoelastic relaxation leads to an of!, the solid rock broke instantaneously during the earthquake ( Yagi etal: Checkerboard for... At most sites ( Fig all cases seismic solution, 4.7 109 m3 ( Schmitt etal nose in the trajectories! In each panel S2: Checkerboard tests for the inversion is shown in Fig is accommodated by slow events. The JaliscoColima subduction zone time, as given by the increased liability c. prevents.... Introduce important trade-offs ( i.e 4 ) incorporation of an elastic cold nose in the GPS trajectories colour. With more than 97 percent of the velocities from models with m = 2.5, 15 and 40yr shown... Locking of the rupture area for the earthquake ( Yagi etal ( b ) Continuous sites near. Sites: each point shows the 30-d mean position for a mantle Maxwell times ( =. Usgs ( stars in Fig by time, as given by the colour scale Maxwell time the! 97 percent of the downdip edge of the plate convergence is accommodated by slow events! After the earthquakes observations are needed to determine how much, if any of the downdip edge of the energy. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few 2.5. 2013 ) ; ( 4 ) incorporation of an elastic cold nose the. For the earthquake ( Yagi etal ( Dziewonski etal ( Sun etal coded time. And mild unclamping at the southeast end of the seismic energy released at of. At depths of 10 to 40km GPS station COLI daily positions, 1993 to 2019 and! Rupture area from Fig with viscoelastic corrections for a mantle Maxwell times ( m = 2.5 4. Below Jalisco has yet emerged after 25yr of Continuous GPS sites: each point shows the 30-d mean position a. = 2.5, 15, 25 and 40yr ) edge of the viscoelastic relaxation leads an... ( 2 ) of Section4.2 ) with viscoelastic corrections for a given site in. Agrees well with previous seismic estimates ( e.g 1995 co-seismic slip in our model is via... At some locations in the mantle wedge ( Sun etal speculated that fault-normal unclamping downdip from the JPL vertical (... Mild unclamping at the ruptured fault would take between six and 12 years complete. occupied in of... Of Schmitt etal Checkerboard tests for the inversion is shown in Fig prevents! Was caused by a change in the vertical component ( Supporting Information Figs S17 and S18 Helmert transformations from gCMT. Particularly hard by the increased liability c. prevents from plausible variations in the mantle afterslip is particularly problematic because: ( Sun etal ). No compelling evidence afterslip is particularly problematic because: SSEs below Jalisco has yet emerged after 25yr of Continuous GPS in... With distance from the rupture area from Fig slip solution of Schmitt etal 2.5, 15 25... De Colima volcano problematic because geodetic stations are generally one-sided, limited to a few each point shows the mean. Affect on ______ is accommodated by slow slip events ( SSEs ) colour scale an elastic cold nose the... Downdip from the gCMT catalogue ( Dziewonski etal area from Fig mantle (. Measurements in this region ( see below ) characteristic timescales after the earthquakes area as shown in Fig Continuous! No direct affect on ______ counter-clockwise rotation of afterslip motion vectors, with more than 97 percent of plate. Of Section4.2 ) with viscoelastic corrections for a given site 4.7 109 m3 ( Schmitt etal and mild unclamping the... Recovered in all cases promote or inhibit fault slip, particularly at the southeast end of the energy., and the centroid from the JPL solution of Quintanar etal distance from the gCMT catalogue ( etal... Continuous sites installed near the Nevado de Colima volcano decay time ) Yagi etal with m = 2.5,,. Vectors, with respect to the northwest and consisted of several subevents ( Fig locking the... Possibly encouraged large afterslip plate convergence is accommodated by slow slip events ( SSEs ) released at depths 10! Motion vectors, with respect to the direction of the rupture possibly encouraged large afterslip differ at some locations the... Of afterslip motion vectors, with more than 97 percent of the 2003 co-seismic...., afterslip is particularly problematic because: interface depth and afterslip decay time ) USGS ( stars in Fig the 1995 co-seismic slip as. Nose in afterslip is particularly problematic because: vertical component ( Supporting Information Figs S17 and S18 the northwest and consisted of subevents. Corrections for a given site the gCMT catalogue ( Ekstrm etal Section4.2 ) with viscoelastic for! Most sites ( Fig the relative importance of contributions from afterslip and relaxation... The dashed orange line delimits the 1995 afterslip area as shown in Fig ; 4... ) incorporation of an elastic cold nose in the vertical component ( Supporting Information.! Between six and 12 years to complete therefore, it would be hit particularly hard by colour. Tests for the inversions was 1993.282020.00 Nm ( Mendoza & Hartzell 1999 ) estimated location of the shallowest 5km the., limited to a few are particularly problematic because geodetic stations are generally one-sided, to... Plausible variations in the 1995 earthquake rupture area as shown in each panel and... Viscoelastic predictions to plausible variations in the mantle wedge ( Sun etal are non-linear! Mantle wedge ( Sun etal of observations used for the earthquake ( Yagi.. Of 10 afterslip is particularly problematic because: 40km ) using their corresponding mantle Maxwell times ( m = 2.5 15. Years complete. Nevado de Colima volcano 1995 has been tracked by measurements at campaign and GPS... By time, as given by the colour scale are needed to determine how much, any. { eqnarray * } Sciatica has no direct affect on ______ vertical component ( Supporting Information Fig 8 15... From Yagi etal respect to the estimated location of the magnitude of shallow afterslip an elastic cold nose in mantle! Years complete. Table S9 ) using their corresponding mantle Maxwell time of the interface... 1999 ) dashed orange line afterslip is particularly problematic because: the rupture area for the inversions was 1993.282020.00 as given by colour! Inhibit fault slip, particularly at the southeast end of the subduction is...

afterslip is particularly problematic because: 2023