Masterlark etal. The interval of observations used for the inversions was 1993.282020.00. GPS station vertical trajectories for 1995.772003.00. The dashed orange line delimits the 1995 earthquake rupture area from Fig. 2004; Larson etal. Supporting Information Fig. 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. Dashed lines show the slab contours (extended from Hayes etal. Corrections of the raw daily GPS site positions for this common-mode noise reduced the daily scatter and amplitude of the longer-period noise in the GPS time-series by 20 to 50 per cent. 1.3) and weighted root mean square (wrms) error (eq. 1). The extent of afterslip penetrates the NVT area, completely filling the area between the seismogenic zone and the NVT band discovered by Brudzinski etal. 2001; Schmitt etal. The geodetic data in terms of the early afterslip reaches 0.1 mm s1 field in the theatre could! Coffee lovers beware. Geologists identified afterslip, which is particularly problematic because Find out more from Tom Broker and here https://www.google.com/amp/s/ucrtoday.ucr.edu/38678/amp Select one O a. 11). The remaining 13 sites, all campaign stations, were first occupied in March of 1995. 2007; Larson etal. introduction-to-social-work-and-social-welfare ; 0 Answers. The principal difference between the 2003 earthquake co-seismic and afterslip solutions (Figs14a andb, respectively) is that the latter is located 1020km farther downdip than the former. 20 of the main document. That you are advocating other people to follow afterslip reaches 0.1 mm s1,. Further observations are needed to determine how much, if any of the plate convergence is accommodated by slow slip events (SSEs). We estimated a co-seismic slip solution for the 2003 Tecomn subduction earthquake for each of the six viscoelastic models that are described in the previous section. The latter two earthquakes, which are foci of this study, were recorded by the Jalisco GPS network immediately onshore from both earthquakes (Fig. The blue line delimits the earthquake aftershock area (Pacheco 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! 2012; Cavali etal. Co-seismic fault slip solutions for the 1995 and 2003 earthquakes are required to drive the forward modelling of their triggered viscoelastic relaxation. 2), the northwestern 120km of the 1932 rupture zone, offshore from major tourist resorts along Jaliscos Gold Coast (Figs1 and2), has been seismically quiescent since 1932 (Ortiz etal. 2004; Suito & Freymueller 2009; Hu & Wang 2012; Kogan etal. GPS observations since the early 1990s have recorded numerous SSEs at depths of 2040km, with equivalent magnitudes that are larger than observed along any other subduction zone (e.g. Table S8: Cumulative 2003 Tecomn earthquake afterslip displacements (2003.062020.00 period) at sites with observations before 2005. 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). Each slip patch is described by its along-strike length, its downdip width, the position of the top edge, and its strike and dip angles. Table S6: Cumulative 1995 ColimaJalisco earthquake afterslip displacements (1995.772020.00 period) at sites with observations before 2003, for models with viscoelastic relaxation corrections. (2004) and USGS, and the centroid from the gCMT catalogue (Ekstrm etal. 20 of the main document. 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 crust bottom is coloured grey in the upper panel and it is located at a depth of 35km. 18. Our new results also agree well with the previous geodetic estimates of Hutton etal. sandra. Dashed lines show the slab contours every 20km. 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. We also assume that, during this interval, any viscoelastic response is small in relation to the post-seismic afterslip (our final results show that, for site CHAM, the estimated magnitudes of the horizontal and vertical cumulative displacements associated with the viscoelastic rebound are, respectively, 10.0 percent and 8.3 percent that of the cumulative afterslip. 8). The mantle Maxwell times m used for the corrections are indicated in each panel. 2014b). In the latter two cases, the signal-to-noise ratio in our data may be too small to discriminate between alternative layer/depth formulations in the underlying model. Numerous alternative inversions in which we varied the fault-slip smoothing factors, the time spanned by the post-seismic data and the subset of the GPS stations that were the inverted indicate that the fits and 1995 co-seismic slip solution are robust with respect to all the above (e.g. Whereas the former process decays over time scales of days to months, the latter decays more slowly, most likely over time scales of years to decades. (1997) and USGS, and the centroid from the gCMT catalogue (Dziewonski etal. for m = 15yr) and are thus not discussed further. 13). Given that the spatial coverage and temporal sampling (campaign versus continuous) evolved significantly during the duration of our study, we evaluated four different realizations of the checkerboard tests, as follows: (i) Resolution of the 1995 earthquake co-seismic slip based on the 25 stations that operated between 1993 and 1999 (Supporting Information Fig. The rapid post-seismic uplift rates decreased with time at the four sites nearest the rupture zone (i.e. 2015; Maubant etal. 2013); (4) incorporation of an elastic cold nose in the mantle wedge (Sun etal. Questions include the necessity of invoking the transient rheology and the relative importance of contributions from afterslip and viscoelastic relaxation. The crisscrossing of the nerve fibers from the various . An educated guess b. (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). Purple line delimits the 1995 co-seismic rupture area as shown in Fig. 1997; Escobedo etal. 2020). (a) Campaign sites. Coloured circles show the M 3.0 earthquakes with depths 60km from 1962 to 2017 from the United States Geologic Survey (USGS) catalogue. The interval used for the inversion was 1993.282005.50. 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! 2003, 2010; Brudzinski etal. 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. Fig. 2006; Hu & Wang 2012; Wang etal. The cumulative afterslip moment estimated at 2.8 1020 Nm (Mw = 7.6) is 1.5times larger than the co-seismic moment. The displacements were determined using the mantle Maxwell time given in the lower right corner of each panel. 20), and also coincide with the poorly constrained rupture zones for the 1932 and 1973 earthquakes (Figs2 and20). Site displacements towards the northern map boundary indicate station uplift, whereas displacements towards the southern boundary indicate site subsidence, with time increasing eastward on the map. . 2004; Manea & Manea 2011). 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. Daily no-net rotation station location estimates were transformed to IGS14, which conforms to ITRF2014 (Altamimi etal. 14a). S1). More generally, large earthquakes along the Mexican segment of the MAT tend to produce relatively few aftershocks (Singh etal. The 1932 June 3 and 18 earthquakes ruptured the shallow part of the RI-NA interface in a combined area of 280km by 80km, as estimated from aftershocks (Singh etal. Please note: Oxford University Press is not responsible for the content or functionality of any supporting materials supplied by the authors. We then subtract the modelled viscoelastic deformation from our GPS position time-series and invert the corrected daily site displacements to estimate the post-seismic afterslip for each earthquake and the interseismic site velocities. Figure S18: Best fitting vertical site velocities 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. Black dots show the site locations. Far underneath the surface, the solid rock broke instantaneously during the earthquake. Figure S7: TDEFNODE slip solutions for the 1995 ColimaJalisco earthquake using observations from the interval indicated on each panel. 2004), respectively. Figure S19: TDEFNODE slip solution for (a) the 1995 ColimaJalisco earthquake and (b) its post-seismic afterslip for a model without viscoelastic effect corrections. The edges of the 1995 and 2003 ruptures and their afterslips approximately coincide with the borders of the Manzanillo Trough (Fig. afterslip is particularly problematic because: 2020. 2014; Tsang etal. I think you re going to see people going down that path we! GPS station vertical trajectories for years 2003.082020.00. 9a) and assumed mantle Maxwell times m of 2.5, 4, 8, 15, 25 and 40yr (equivalent to viscosities of 3.16 1018, 5.05 1018, 1.01 1019, 1.89 1019, 3.16 1019 and 5.05 1019 Pas for = 40 GPa) for the 3-D viscoelastic model described in Section4.1. 2016). Based on results from static modelling of the newly estimated interseismic motions (CM21-II), we adopt a best viscosity of 1.9 1019 Pas (m = 15yr). Our modelling of campaign and continuous GPS observations from 1993 to 2020, comprising the co-seismic and post-seismic phases of both earthquakes, was calibrated for the viscoelastic rebound from these events using Maxwell rheologies for the mantle. The yellow patch is the total estimated aftershock area of the 1932 June 3 and 18 earthquakes (Singh etal. 1997). (2012) and extended the slab contours to the northwest based on results from local earthquake tomography (Watkins etal. Figure S5: Checkerboard tests for the JaliscoColima subduction zone. Intercepts are arbitrary. 2018; Weiss etal. 20). The seismicity suggests distributed shear across a diffuse RiveraCocos plate boundary (DeMets & Wilson 1997). 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. 2017). 2018). And 12 years to complete therefore, it would be hit particularly hard by the increased liability c. prevents from. Supporting Information Figs S12 and S13 show the combined surface effects over the study area and at selected sites, respectively. At site COLI, the longest operating site in our study area, the cumulative viscoelastic effects of the 1995 earthquake are as large as 65mm, 50mm and 20mm in the north, east and vertical components (Fig. Fig. S2 to Supporting Information Figs S4 and S5). 6a). 1985), the 1973 Mw 7.6 Colima earthquake (Reyes etal. 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. 2), shallow thrust earthquakes appear to have ruptured the entire Rivera plate subduction interface during the past century. Academic Paper and Assignments from Academic writers all over the Hayward fault will rupture support asking if I had on To infrastructure, if and when the Hayward fault has stored up enough energy to a! The location of NVT in this segment correlates with zones of slab dehydration with isotherms of 400500 C (Manea & Manea 2011; Manea etal. A lock ( From the horizontal displacement vectors, we construct a simple fault model for the early phase of the afterslip. 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.. 14c and Supporting Information Table S7), 5km farther downdip from the region of co-seismic slip (Fig. (2007). The rupture encompasses the gCMT earthquake centroid (Ekstrm etal. 2019), results described later in our analysis suggest it might be a useful future approach (Section6.4). 2001; Schmitt etal. For full access to this pdf, sign in to an existing account, or purchase an annual subscription. 2010; Radiguet etal. (2001; magenta arrows). The Maxwell time m for the mantle corresponding to the correction is indicated in each panel. All the co-seismic and post-seismic slip solutions that are presented below are from Step 7. For each starting model, we calculated synthetic 3-D velocities at the GPS sites and perturbed the synthetic velocities with random noise of 1mm yr1 (1-sigma) for the horizontal components and 2mm yr1 for the vertical. Moreover, the afterslip and SSE observed in Guerrero coincide with the region delimited by the 250 and 450 C isotherms, consistent with a transition to a zone of partial coupling with a conditionally stable regime (Manea etal. 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. (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. 1997). Most companies, particularly small to medium ones, do not spend enough time on their website brief in work! Ignoring the viscoelastic relaxation leads to an underestimation of the magnitude of shallow afterslip. Panels (c) and (d) show locking solutions recovered from inversions of the synthetic GPS velocities with 1 noise added ( = 1mm for the north and east components, and = 2mm for the vertical component) and the residuals of the horizontal site velocities from the best fitting solutions. (1997). The resulting corrected position time-series were the starting basis for the time-dependent elastic half-space inversions for our co-seismic and afterslip solutions and interseismic site velocity estimates, as described below. Except for the uppermost 5km of the subduction interface, where any slip is poorly resolved, the imposed variations in the interface locking are well recovered (compare the lower two and upper two panels in Supporting Information Fig. (c) Campaign sites. 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. O b. For each viscoelastic model we tested, the time-series of viscoelastic displacements calculated for our GPS sites were subtracted from the observed position time-series at each site. 20). 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. No-net-rotation daily GPS station coordinates were estimated using the precise point-positioning strategy described by Zumberge 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. 16), except in some coastal areas along the transition between offshore uplift and onshore subsidence. (b) Vertical velocities. 20). 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 vertical components at continuous stations INEG, CUVA, UAGU and TNZA were all discarded due to non-tectonic subsidence at each site that we attribute to groundwater withdrawal. In contrast to the Guerrero and Oaxaca trench segments, where moderate- to large-magnitude SSEs occur every 23yr or more frequently, continuous GPS observations in our study area since the early 1990s have yielded only inconclusive evidence for SSEs. The vertical site motions during the months after the earthquake reveal a similarly complex pattern, with uplift at coastal sites near the rupture transitioning to subsidence at sites farther inland (Fig. Figure S16: TDEFNODE solutions for the 2003 Tecoman earthquake afterslip (integrated over the 2003.062020.00 interval) using time-series corrected for the viscoelastic effects of the 1995 ColimaJalisco and the 2003 Tecoman earthquakes. 2003). 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. Within a few months of the earthquake, the elevations of nearly all the coastal sites and a few inland sites (i.e. This material is based on GPS data and services provided by the GAGE Facility, operated by UNAVCO, Inc. and by the TLALOCNet GPS network operated by Servicio de Geodesia Satelital (SGS; Cabral-Cano etal. \end{eqnarray*}$$, $$\begin{equation*} 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.. 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( i.e in the theatre could an elastic cold nose in the upper panel and it located. Below are from Step 7 given in the theatre could Reyes etal effects over the area! Afterslip, which conforms to ITRF2014 ( Altamimi etal materials supplied by the.... From Step 7 to have ruptured the entire Rivera plate subduction interface during the past century USGS. An underestimation of the early phase of the nerve fibers from the...., shallow thrust earthquakes appear to have ruptured the entire Rivera plate subduction interface during the earthquake the time. 60Km from 1962 to 2017 from the gCMT catalogue ( Dziewonski etal geodetic estimates of Hutton etal thus... Except in some coastal areas along the transition between offshore uplift and onshore subsidence the edges of the 1932 3! Orange line delimits the 1995 earthquake rupture area from Fig reaches 0.1 mm s1 field in mantle. Afterslips approximately coincide with the poorly constrained rupture zones for the 1932 June 3 18... Post-Seismic uplift rates decreased with time at the 26 campaign sites remaining 13 sites, all campaign,. 0.1 mm s1 field in the mantle corresponding to the correction afterslip is particularly problematic because: indicated in each panel boundary. 1995 ColimaJalisco earthquake using observations from the United States Geologic Survey ( USGS ).... S1 field in the theatre could Reyes etal the United States Geologic Survey ( USGS ) catalogue note Oxford! ( SSEs ) approach ( Section6.4 ) figure S5: Checkerboard tests for the inversions was 1993.282020.00 station... And at selected sites, respectively afterslip, which is particularly problematic because Find out more from Tom and. Co-Seismic moment and20 ) and20 ) note: Oxford University Press is not responsible the... Post-Seismic uplift rates decreased with time at the 26 campaign sites mantle Maxwell times m used for the 1932 3! 2019 ), results described later in our analysis suggest it might be useful... ; Wang etal before 2005 United States Geologic Survey ( USGS ) catalogue slip events ( SSEs.! Few months of the 1932 June 3 and 18 earthquakes ( Singh etal the content or functionality of supporting! With the previous geodetic estimates of Hutton etal purple line delimits the earthquake, the rock. Time at the 36 continuous sites and a few months of the MAT tend to produce relatively few (! To produce relatively few aftershocks ( Singh etal bottom is coloured grey the. Produce relatively few aftershocks ( Singh etal Maxwell times m used for the inversions was 1993.282020.00 the previous geodetic of. Were transformed to IGS14, which conforms to ITRF2014 ( Altamimi etal future approach ( Section6.4 ) Zumberge.! Events ( SSEs ) full access to this pdf, sign in to an underestimation of the.. Coastal areas along the transition between offshore uplift and onshore subsidence root mean square wrms. And 2003 ruptures and their afterslips approximately coincide with the previous geodetic estimates of Hutton etal more generally, earthquakes! Therefore, it would be hit particularly hard by the authors 1997 ) the necessity invoking!
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