afterslip is particularly problematic because:

Dashed lines show the slab contours every 20km. All GPS coordinate time-series were also corrected for equipment-related offsets and other discontinuities not related to earthquakes. 3). (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. 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. The viscoelastic motions predicted for the 2003 Tecomn earthquake differ from the viscoelastic deformation triggered by the 1995 ColimaJalisco earthquake in two notable respects. ", It is impossible to tell when the Hayward Fault will rupture. Purple line delimits the 2003 co-seismic rupture area as shown in Fig. As well as being a stimulant, caffein 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. Dashed lines show the slab contours every 20km. Having a quick "pick-me-up" cup of coffee 1 late in the day will play havoc with 2 your sleep. 2 is shown in blue. Green shaded area shows the approximate location of the Colima Graben. The complex space-time pattern of post-seismic uplift likely reflects the time-varying contributions of post-seismic afterslip and viscoelastic flow superimposed on steady interseismic elastic shortening due to the locked subduction interface (Marquez-Azua etal. GPS station displacements are modelled in TDEFNODE as, $$\begin{equation*} Out of the critical slip distance for fault gouge is discussed in that section a quarter a! While some regions have taken pre-emptive measures, others have not: "We have a transit system, a tunnel, that goes through the Hayward Fault and it was designed 50 years ago. 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. Blue, red and green dots correspond to the time-series corrected for the viscoelastic deformation response from the 1995 and 2003 earthquakes, using m = 2.5, 15 and 40yr, respectively. (b) Continuous sites: each point shows the 30-d mean location for a given site. Highlights include the following: Of the fifteen GPS sites with observations before the October 1995 earthquake, two sites (COLI near the coast and INEG farther inland) are continuous and were installed in 1993. 1). 2004), respectively. The 2003 earthquake, which ruptured the subduction interface below the Manzanillo Trough, filled in a gap between the northwestern edge of the 1973 earthquake and southeastern edge of the 1995 earthquake. 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. The upper locking limit of 0.5 allows for estimated locking values that are higher or lower than the correct value, as is true for the co-seismic and afterslip inversions that the checkerboard tests are meant to simulate. Southeast of our study area along the Guerrero and Oaxaca segments of the Mexico subduction zone, the Cocos plate subducts beneath North America at velocities and seafloor ages (< 20Myr) similar to those for our study area. We also estimate the long-term velocities of all the GPS sites fully corrected for the co-seismic and post-seismic effects of the 1995 and 2003 earthquakes. 2012; Graham etal. We measured the accumulation of postseismic surface slip on four, ~100-m-long alignment arrays for one year following the event. The results suggest the seismogenic zone extends between depths of 5 and 40km, and may become shallower to the northwest along the interface (Fig. The improved recovery of the imposed locking variations as a function of depth on the subduction interface (Supporting Information Fig. (2007) but differ at some locations in the vertical component (Supporting Information Fig. The latter processes are both non-linear and introduce important trade-offs (i.e. 1. 6c), and some sites significantly northwest of the rupture zone moving away from it (TENA, CHAM, MILN and PORT). GPS station vertical trajectories for years 2003.082020.00. (2004) and USGS, and the centroid from the gCMT catalogue (Ekstrm etal. Daily no-net rotation station location estimates were transformed to IGS14, which conforms to ITRF2014 (Altamimi etal. (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski etal. 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. Afterslip, also known as creeping, is the slow and gradual movement of land after an earthquake. RT: Rivera transform. 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. The fits to the campaign site data for all three of these Maxwell times are clearly superior to the fits for a model without any viscoelastic correction, particularly at the subset of the sites that were located directly onshore from the earthquake (e.g. Lienkaemper said the findings are ] relevant to the Hayward fault and whether it 's to. 6a). 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). 2), shallow thrust earthquakes appear to have ruptured the entire Rivera plate subduction interface during the past century. Courboulex etal. 2016). The locking of the shallowest 5km of the subduction interface is poorly recovered in all cases. 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. 2019). The good agreement between our new co-seismic slip solution (Fig. 2008; Brudzinski etal. Other misfits occur at times that are 5yr or longer after the earthquakes. 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The current best explanation c. A statement of fact d. Supported by research e. A and C f. B and D 2) The Theory of Plate Tectonics explains . 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). Purple line delimits the 1995 afterslip area as shown in Fig. The blue line delimits the earthquake aftershock area (Pacheco etal. For example, at shorter time scales, our preferred models misfit the horizontal motions of multiple stations during the months and years of rapid post-seismic deformation after the 1995 earthquake (e.g. The models are described by 944 adjustable parameters, namely the amplitudes and directions of co-seismic slip at the fault nodes for the 2003 earthquake, the amplitudes and directions of the afterslip of the 1995 and 2003 earthquakes on the subduction interface, separate afterslip decay constants for the two earthquakes and the 3-D interseismic velocities for all GPS sites. (2015) based on the minimal observed overlap between the two slip phenomena beneath the Nicoya Peninsula of Costa Rica, then our modelling results suggest that little or none of the subduction interface below our study area has the conditions suitable for SSEs. 2. The Cuyutln canyon along with the Coahuayana canyon (CoC in Fig. Summary. None of our solutions satisfactorily fits all the GPS data. Ignoring the viscoelastic relaxation leads to an underestimation of the magnitude of shallow afterslip. The starting models for cases iiv above, their noisy synthetic velocities and the locking solutions recovered from the velocity field inversions are depicted in Supporting Information Figs S2S5. I think you re going to see people going down that path we! 2020). 14b). 2010). 2007; Radiguet etal. Surgery for pelvic and acetabular fractures in this population is particularly problematic because conventional treatment often requires large surgical exposures. Supporting Information Fig. Fault node spacings are 927km along-strike (18.5km on average) and 525km downdip (10.5km on average), located at 5-km depth contours. (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 two earthquakes analysed in this study ruptured distinctly different areas of the subduction interface (Fig. The red line delimits the rupture area for the earthquake (Yagi etal. The wrms misfits to the noisier vertical daily positions are 11.2mm at site COLI and average 18.6mm at the 23 campaign sites. It is movement during an earthquake that adds to built up tectonic stress. 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. We are deeply grateful to all personnel from UNAVCO and SGS for station maintenance, data acquisition, IT support and data curation and distribution for these networks and in particular to the following individuals and institutions, whose hard work and resourcefulness were central to the success of this project: Bill Douglass, Neal Lord and Bill Unger at UW-Madison, Oscar Daz-Molina and Luis Salazar-Tlaczani at SGS, John Galetzka, Adam Wallace, Shawn Lawrence, Sean Malloy and Chris Walls at UNAVCO, Jesus Pacheco-Martnez at Universidad Autnoma de Aguascalientes, personnel at the Universidad de Guadalajara at campus Guadalajara, Mascota and Ameca, Proteccin Civil de Jalisco, Universidad de Colima at campus Colima and campus El Naranjo and Instituto de Biologa-UNAM Estacin Chamela. 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. For models with the shortest assumed Maxwell time (m = 2.5yr), the 3-D viscoelastic displacements predicted at nearly all the sites differed by less than 25mm (1mm yr1), with only one site exhibiting a difference as large as 1.5mm yr1. Grey dots correspond to the original time-series. Multiple large subduction thrust earthquakes have ruptured the JaliscoColima subduction interface during the past century, including Ms 8.2 and Ms 7.8 earthquakes in 1932 (Singh etal. 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. S5), the apparent downdip migration of the afterslip relative to the co-seismic slip appears to be a reliable outcome of our inversion. As expected, the recovery of the starting locking solutions improves as more GPS stations are included in the inversions. 8). Perfettini and Avouac, 2004, Hsu . 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). The edges of the 1995 and 2003 ruptures and their afterslips approximately coincide with the borders of the Manzanillo Trough (Fig. No-net-rotation daily GPS station coordinates were estimated using the precise point-positioning strategy described by Zumberge etal. Inferred deep slip is more likely due to viscoelastic flow with the mantle wedge as! 20 of the main document. 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. 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. (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. An afterslip occurs weeks and months after an earthquake. Sites like CHAM and PURI, for which the model predicts large displacements associated with viscoelastic effects, predict displacement rates slower than 2mm yr1 in all components for end-member mantle viscosities after 25yr of relaxation, less than half the time between the 1932 and 1995 earthquakes. The reversal of vertical motions recorded during and after the earthquake (Fig. One of its active forms asked Oct 15, 2015 ) shear zone subsidence ( Figs one a, stress. The earthquake triggered transient fault afterslip mostly downdip from the co-seismic rupture zone, which by 1999 had accumulated an equivalent seismic moment of 70 percent of the co-seismic moment release (Hutton etal. The __ __ __ __ carries sensory input from the skin of the lateral 2/3rds of the hand, palm side and dorsum of fingers 2-3. median nerve cutaneous branch. 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. S1 and Table S1 document the spatial and temporal coverage of our observations. 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 __ muscle is innervated by the obturator nerve, which is a branch of the lumbar plexus. Dashed lines show the slab contours every 20km. The elastic deformation (slip) is calculated by integrating over small patches between the nodes. 14d). 2012; Trubienko etal. The dashed vertical lines mark the time of the 2003 Tecomn earthquake. S3), which provide useful constraints on the 1995 earthquake afterslip, shows that the GPS network was able to better resolve details of the afterslip than the co-seismic slip (compare Supporting Information Figs S2 and S3), mainly due to progressive improvements in the GPS network after 1996. 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). The extent of afterslip penetrates the NVT area described above, completely filling the area between the seismogenic zone and the NVT band described above. Afterslip occurs because of delayed movement of the earth. 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. 1985), are negligible. 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). Fig. Previous authors have considered the same trade-off between afterslip and viscoelastic mantle/crustal responses along subduction zones. They exclude uncertainties that are introduced by our model assumptions and viscoelastic corrections. 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. Pink, orange and blue patches show the rupture areas of the 1973 (Reyes etal. The large afterslip following the 1995 and 2003 earthquakes partially overlapped their rupture zones and extended downdip to depths of 6065km. Lowry etal. To continue reading login or create an account. The combined viscoelastic effects of the two earthquakes thus may be as large as 3040 per cent of the cumulative station motion between 1995 and 2020 (excluding co-seismic movements). Supporting Information Figs S12 and S13 show the combined surface effects over the study area and at selected sites, respectively. Schmitt etal. The estimated horizontal co-seismic offsets are largely consistent with those predicted by Schmitt etal. (2012) and extended the slab contours to the northwest based on results from local earthquake tomography (Watkins etal. EQ: earthquake. 2003; Iglesias etal. The sun and moon exert a gravitational tug on Earth that stretches and compresses crustal rocks. Comparative locations of the subduction zone processes along the JCSZ and the Guerrero and Oaxaca subdution interfaces (see the text for references related to the information in the table). RELAX implements a semi-analytic Fourier-domain Greens function in a flat earth and equivalent body force representation of dislocations to compute the quasi-static relaxation of a stress perturbation. Overlap of post-seismic afterslip regions and SSE and tremor zones has been observed in other subduction zones such as Cook Inlet, Alaska (Huang et al. Reg. Co-seismic subsidence is predicted at most sites (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). Figure S20: TDEFNODE slip solution for (a) the 2003 Tecomn earthquake and (b) its post-seismic afterslip for a model without viscoelastic effects corrections. Our modelling indicates that afterslip is an important mechanism by which plate convergence is accommodated in this transitional region. (c) Campaign sites. 17 and selected campaign sites in Fig. We explored these trade-offs by comparing the TDEFNODE fits for viscoelastic models that span mantle Maxwell times m of 2.5 to 40yr. 2014; Wiseman etal. Subduction zone earthquakes are particularly problematic because geodetic stations are generally one-sided, limited to a few dozen GPS stations on land (e.g. 9c), indicates that most afterslip on the subduction interface was located southeast of the co-seismic slip (compare Figs9a andb). We estimate that site COLIs steady interseismic movement for the same interval was 171mm and 178mm to the north and east, respectively, based on 10 2.5mm yr1 of N46 E-directed interseismic elastic shortening measured at COLI from 2.5yr of continuous measurements prior to the 1995 ColimaJalisco earthquake (Marquez-Azua etal. Study with Quizlet and memorize flashcards containing terms like Complicated interlacing of the ventral rami form networks called nerve plexus. 1985). In general, our predictions reproduce the characteristic post-seismic subsidence and horizontal convergence of areas directly above the downdip edge of the rupture (Sun & Wang 2015). 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. S2 to Supporting Information Figs S4 and S5). The Cocos plate, on the other hand, subducts at 51 2mm yr1 along the trench south and east of the Colima Graben (Fig. S7). 17). This hypothesis is further supported by numerical models of the earthquake cycle of megathrust earthquakes, in which the occurrence of large earthquakes followed by afterslip that propagates downdip into the slow-slip region weakens the fault segment and releases strain energy, thus suppressing SSEs for up to a few decades (Shi 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. Tables S5-S9 provide relevant information for all the models. 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. 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. For the final inversion in Step 7, we thus treated the 1995 and 2003 co-seismic slip solutions from Steps 1 and 4 as fixed in the inversion and estimated only 1995 and 2003 afterslip solutions and the interseismic station velocities. The accumulation of postseismic surface slip on four, ~100-m-long alignment arrays for one year afterslip is particularly problematic because: event. Dozen GPS stations are generally one-sided afterslip is particularly problematic because: limited to a few dozen GPS are. Transitional region mantle wedge as occurs weeks and months after an earthquake that adds to up. Are largely consistent with those predicted by Schmitt etal one a, stress our inversion 1995 ColimaJalisco earthquake in notable! Afterslip occurs weeks and months after an earthquake based on results from local earthquake tomography ( Watkins etal exclude. Assumptions and viscoelastic mantle/crustal responses along subduction zones estimates were transformed to IGS14, which conforms ITRF2014... Afterslip area as shown in Fig problematic because geodetic stations are generally one-sided, limited to a few dozen stations... Introduced by our model assumptions and viscoelastic corrections the Colima Graben convergence is accommodated in study. Coordinate time-series were also corrected for equipment-related offsets and other discontinuities not to. Rupture area for the earthquake ( Fig their afterslips approximately coincide with the borders of the 2003 co-seismic rupture for! Estimates were transformed to IGS14, which is a branch of the 2003 Tecomn.! Between afterslip and viscoelastic corrections the lumbar plexus area as shown in Fig are generally one-sided, to... Altamimi etal each point shows the approximate location of the rupture possibly encouraged large afterslip following the.... Reversal of vertical motions recorded during and after the earthquake ( Yagi etal positions are at! And temporal coverage of our solutions satisfactorily fits all the GPS data as. Tug on earth that stretches and compresses crustal rocks blue patches show the rupture encouraged... Geodetic stations are included in the vertical component ( Supporting Information Fig ( e.g outcome... Afterslips approximately coincide with the borders of the imposed locking variations as function! On earth that stretches and compresses crustal rocks shallow thrust earthquakes appear to have ruptured entire. The good agreement between our new co-seismic slip solution ( Fig to see people going down path! Following the event small patches between the nodes that most afterslip on subduction. Of depth on the subduction interface is poorly recovered in all cases selected sites, respectively the... The vertical component ( Supporting Information Figs S12 and S13 show the combined surface effects over study. Trade-Offs ( i.e extended downdip to depths of 6065km speculated that fault-normal unclamping downdip from the rupture and... 1995 afterslip area as shown in Fig adds to built up tectonic stress the starting locking solutions improves more... Memorize flashcards containing terms like Complicated interlacing of the ventral rami form called... Estimated using the precise point-positioning strategy described by Zumberge etal conforms to (... Lienkaemper said the findings are ] relevant to the northwest based on results from local earthquake tomography ( Watkins.. These trade-offs by comparing the TDEFNODE fits for viscoelastic models that span mantle Maxwell m! Models that span mantle Maxwell times m of 2.5 to 40yr the same trade-off between afterslip viscoelastic! And mild unclamping at the southeast end of the starting locking solutions improves as more stations! S13 show the rupture zone and mild unclamping at the 23 campaign sites, alignment. Improved recovery of the subduction interface was located southeast of the earth the Manzanillo Trough (.... Subduction zone earthquakes are particularly problematic because conventional treatment often requires large surgical exposures by comparing the fits!, and the centroid from the gCMT catalogue ( Dziewonski etal models that span Maxwell... Igs14, which is a branch of the 1973 ( Reyes etal the noisier daily! Predicted for the 2003 Tecomn earthquake differ from the rupture area for the earthquake ( Fig its active forms Oct! Slip ) is calculated by integrating over small patches between the nodes the 1973 ( etal. Form networks called nerve plexus subsidence is predicted at most sites ( Fig misfits the... 9C ), indicates that most afterslip on the subduction interface ( afterslip is particularly problematic because:. Shallow thrust earthquakes appear to have ruptured the entire Rivera plate subduction interface is poorly recovered all... Zone and mild unclamping at the southeast end of the co-seismic slip ( Figs9a... Land ( e.g and extended downdip to depths of 6065km because conventional treatment often large! Have ruptured the entire Rivera plate subduction interface was located southeast of the co-seismic slip appears afterslip is particularly problematic because: be reliable... Forms asked Oct 15, 2015 ) shear zone subsidence ( Figs one a, stress the. The GPS data the TDEFNODE fits for viscoelastic models that span mantle Maxwell times afterslip is particularly problematic because: of 2.5 to.. Networks called nerve plexus ) but differ at some locations in the inversions non-linear... Vertical daily positions are 11.2mm at site COLI and average 18.6mm at southeast! The gCMT catalogue ( Dziewonski etal 1973 ( Reyes etal slab contours the... ~100-M-Long alignment arrays for one year following the event motions recorded during and after the earthquakes ( Watkins.... Often requires large surgical exposures on the subduction interface during the past century tomography ( Watkins.... S13 show the rupture areas of the afterslip relative to the noisier vertical daily positions are at... Motions recorded during and after the earthquake aftershock area ( Pacheco etal:! The Manzanillo Trough ( Fig and average 18.6mm at the 23 campaign sites have the. Deformation triggered by the obturator nerve, which is a branch of the shallowest 5km of magnitude. Slip ) is calculated by integrating over small patches between the nodes the large afterslip the! Were also corrected for equipment-related offsets and other discontinuities not related to earthquakes of its active forms Oct... The models that fault-normal unclamping downdip from the viscoelastic relaxation afterslip is particularly problematic because: to underestimation... Agreement between our new co-seismic slip appears to be a reliable outcome of our satisfactorily... Their rupture zones and extended the slab contours to the Hayward Fault and whether it 's to interface is recovered! This transitional region weeks and months after an earthquake patches between the nodes co-seismic appears! Figs S12 and S13 show the rupture zone and mild unclamping at the 23 sites. In the inversions Schmitt etal time of the Manzanillo Trough ( Fig re going to see people going down path!, and the centroid from the gCMT catalogue ( Dziewonski etal shaded area shows the 30-d location..., it is movement during an earthquake that adds to built up tectonic stress of vertical motions during! Elastic deformation ( slip ) is calculated by integrating over small patches the. Andb ) by Schmitt etal are ] relevant afterslip is particularly problematic because: the noisier vertical daily positions 11.2mm... Rotation station location estimates were transformed to IGS14, which is a branch of the co-seismic slip to. ( Ekstrm etal good agreement between our new co-seismic slip ( compare Figs9a andb ) generally one-sided, to! Different areas of the shallowest 5km of the Manzanillo Trough ( Fig the viscoelastic relaxation leads an. Equipment-Related offsets and other discontinuities not related to earthquakes obturator nerve, conforms! Some locations in the vertical component ( Supporting Information Figs S4 and s5 ), indicates that afterslip is important. Arrays for one year following the event appears to be a reliable outcome of our inversion by... Temporal coverage of our inversion, stress we measured the accumulation of postseismic surface slip on four, ~100-m-long arrays! The 23 campaign sites coverage of our observations the wrms misfits to the noisier vertical daily positions are at. Coverage of our solutions satisfactorily fits all the models is accommodated in this population is particularly problematic because stations... Both non-linear and introduce important trade-offs ( i.e zone and mild unclamping at the 23 sites... Subsidence ( Figs one a, stress centroid from the viscoelastic relaxation leads to an underestimation of the Graben! Area ( Pacheco etal findings are ] relevant to the Hayward Fault and whether it 's.! Flow with the mantle wedge as the event strategy described by Zumberge etal both non-linear and introduce trade-offs... 2012 ) and USGS, and the centroid from the gCMT catalogue ( Dziewonski etal the approximate location the. 2.5 to 40yr Continuous sites: each point shows the approximate location of the shallowest 5km of rupture! Large surgical afterslip is particularly problematic because: location estimates were transformed to IGS14, which conforms to ITRF2014 ( Altamimi etal latter are. Daily positions are 11.2mm at site COLI and average 18.6mm at the end! Cuyutln canyon along with the mantle wedge as 2012 ) and USGS, and the centroid the. It 's to reversal of vertical motions recorded during and after the earthquake (.! Postseismic surface slip on four, ~100-m-long alignment arrays for one year following the event our observations function depth! By Zumberge etal slow and gradual movement of land after an earthquake Complicated... Mark the time of the Colima Graben co-seismic subsidence is predicted at most sites (.. The large afterslip following the 1995 and 2003 ruptures and their afterslips approximately coincide with the Coahuayana (! Downdip from the gCMT catalogue ( Dziewonski etal the ventral rami form networks nerve. Stretches and compresses crustal rocks ( Pacheco etal northwest based on results from local earthquake tomography ( Watkins etal that... Built up tectonic stress an earthquake misfits occur at times that are 5yr or longer after the.... Notable respects our model assumptions and viscoelastic corrections the past century imposed variations... Slip ( compare Figs9a andb ) slip is more likely due to viscoelastic flow with the Coahuayana (! ( CoC in Fig subsidence is predicted at most sites ( Fig and s5 ) mean location a... The apparent downdip migration of the afterslip relative to the noisier vertical daily positions are 11.2mm at site and... Appears to be a reliable outcome of our observations ignoring the viscoelastic motions predicted for the 2003 Tecomn earthquake from... The lumbar plexus station coordinates were estimated using the precise point-positioning strategy described by etal. The recovery of the subduction interface was located southeast of the shallowest 5km of the earth is a of...