Bingmin S.-T.. Friedrich A.M. Wernicke B. Niemi N.A. The surface where they slip is called the fault or fault plane. The stress field changes with time (Hardebeck & Hauksson 2001a, and Section 4.4) and is not necessarily identical to the long-term loading rates over several million years, or the loading rates predicted by our block model. An extension of this approach, in which one solves for individual Euler vectors for each block, was applied to the eastern California shear zone by McClusky et al. Pollitz 2003). Note* The earthquake faults are color coded by unique name and section not type. Another robust feature if we allowed for regional variations in dl was a shallow locking depth in the Salton Trough. 2). Compared with the previous SCEC crustal velocity map, the new set has 400 more data points and much improved spatial coverage. In a next step, we will then use the stresses for a joint inversion for fault slip rates. Our choice of fault locations was primarily guided by mapped surface traces along the major strands of the SAF system (after Jennings 1975). Since we are aiming for a regional representation of crustal stress, we include a flatness constraint for the inversion, minimizing the difference between stress tensor components at adjacent gridpoints (Fig. (1990) and Dorsey (2002); (4) van der Woerd et al. Horizontal components of scaled stresses from an inversion including focal mechanisms after Landers (filled sticks, compare with Fig. Sci., USSR, Phys. The upper time limit for initiation of faulting is constrained by the crystallization age of the primary rock type (known as "Kristallgranit") at 325 7 Ma, whereas the K-Ar and Rb-Sr ages of two illite fractions <2 m (266-255 Ma) are interpreted to date fluid infiltration events during the final stage of the cataclastic deformation period. Hauksson 2000). The alignment of strain rates and seismicity inversion results we find would be consistent with a situation in which the non-tectonic background stress is large in amplitude compared with the loading stress, but fluctuating widely. Rockwell T.K. 1. When an earthquake occurs on one of these faults, the rock on one side of the fault slips with respect to the other. 2001), leading us to expect significant viscoelastic effects (cf.McClusky et al. Since the amplitude of stress is not constrained, however, we proceed as follows: solve for block motions using eq. The major strike-slip motion of the plate boundary in Fig. - Well-constrained fault - Moderately constrained fault - Inferred fault In the problem, we are given a set of sites equipped with an unconstrained number of facilities as resources, and a set of clients with set \mathcal {R} as corresponding connection requirements, where every facility belonging to . Sieh et al. Fine lines denote the fault trace of the Landers 1992 event (243.5E/34.3N, see Figs 2 and 11). Stresses, in turn, might vary at all length scales such that the inherent or explicit smoothing of both the stress inversions and the moment summation might have no relevance for the loading state close to the fault. Shaw & Shearer 1999; Plesch et al. The fault surface can be vertical, horizontal, or at some angle to the surface of the earth. Ground shaking is the primary cause of earthquake damage to man-made structures. However, fault segments that show slow apparent slip in the half-space model (such as the San Andreas SBM segment, see Section 3.1) may alternatively be interpreted as being late in the seismic cycle (Savage & Lisowski 1998). Zoback 1992; Reinecker et al. Most often asked questions related to bitcoin. Mapped scale will control visualization of the fault at various scales. The mean velocity misfit of this model, |v|>, is 2.1 mm yr-1 (1.4 mm yr-1 component-wise). However, both plots show that the slip rate of the fault is less well constrained, which may contribute to the relatively high slip rate in the best-fitting fault model. If you continue to use this site we will assume that you are happy with it. In this model, interseismic crustal deformation is solely generated by faults that are locked down to an aseismic depth. Am., Cordilleran Section, Abstracts with Programs, Numerical Recipes in C: The Art of Scientific Computing, Neotectonics of the San Cayetano Fault, Transverse Ranges, California, Late Quaternary rate of slip along the San Jacinto fault zone near Anza, southern California, Paleoseismology of the Johnson Valley, Kickapoo, and Homestead Valley faults: clustering of earthquakes in the Eastern California Shear Zone, Equivalent strike-slip earthquake cycles in half-space and lithosphereasthenosphere Earth models, Geodetic determination of relative plate motion in central California, Viscoelastic coupling model of the San Andreas fault along the Big Bend, Southern California, Quaternary dextral fault slip history along the White Mountains fault zone, California (abstract), 98th Ann. During the inversion, we allow block L to readjust the reference frame by treating the long-term block motion, L, as a free parameter (see Section 2.3.1 and Tables A1 and A2). Our block geometry is such that there are at least eight data points in each block, with fewest sites in block C. Seven out of the total of 540 GPS points of our edited SCEC data set are outside the study region, as shown in Fig. The authors argue that the relative motions between crustal blocks can be well explained by smooth basal velocity gradients driving a system without significant interseismic strain accumulation in the brittle-elastic part of the lithosphere. For big earthquakes this might go on for decades. 2003). Three earthquakes in this sequence had a magnitude (M) of 7.0 or greater. A fault is a thin zone of crushed rock separating blocks of the earth's crust. These fault segments are given a different value for name, number, code, or dip direction and so in the database each segment occurs as its own unique entity. Table 1 compares our predicted fault slip rates for = 0 and = 1 with selected palaeoseismological and geomorphological rate estimates (see Table caption for references). The scale for slip rates [different for (a) and (b)] and residual velocities is indicated along with the mean residual velocity vector length, v, and the component-wise mean misfit (in brackets). Lucy Jones on Twitter: " [email protected] A "well-constrained" fault has a clear expression at Earth's surface, not covered by sediment, so we know just where it is" Since the formation of the San Andreas Fault system 25-30 million years ago, the juxtaposition of the Pacific and North American plates has formed many faults in California With innovations, fresh data, and lessons learned from recent earthquakes, scientists have developed a new earthquake forecast model for California, a region under constant threat from potentially damaging events. 9 shows 2 misfits versus regionally constant locking (or fault segment) depth. (2001) and to the Marmara sea by Meade et al. Embrace the greens and . 1994), PAC-NAM, and have larger amplitudes (Table A2). Souter B.J.. Meade B.J. CONCLUSIONS Surface faulting is affected by: fault characteristics overlying soil foundation & structure Effects of surface fault rupture can be acceptable or unacceptable Surface fault rupture can be analyzed and Thrust motion is instead placed on the SBM region (11 mm yr-1). Our approach of velocity modelling follows Meade et al. Fig. The same process goes on in an earthquake. Epicenter, hypocenter, aftershock, foreshock, fault, fault plane, seismograph, P-waves, magnitude, intensity, peak acceleration, amplification We hear them. Very little slip is transferred between these two systems, resulting in a low (<10 mm yr-1) slip on the SMB segment of the SAF, less than in either of the previously proposed models. Is one available in GIS format? have occurred as few as 45 years and as many as 300 years apart. (2003) identified as potential outliers, possibly related to site or post-seismic effects (Fig. This finding is consistent with the time dependence of stresses close to a fault during the seismic cycle, where we expect rotation towards a more fault-perpendicular angle after stresses are released (e.g. 2002a). USGS Earthquake Hazards Program, responsible for monitoring, reporting, and researching earthquakes and earthquake hazards San Cayetano, Cucamunga, and Sierra Madre faults show thrust rates of 1-8 mm yr-1 (Rockwell 1988), 3-5 mm yr-1 (Walls et al. Some selected long-term slip rates derived from are listed in the left part of Table 1 and sorted by fault segment codes as shown in Fig. North of the SBM, the Mojave segment of the SAF accommodates 9-16 mm yr-1, while the ECSZ also has 15-18 mm yr-1 rates. Bonkowski M.S. Shaded circles are plotted at the centre of each dislocation patch and scale with the slip rate. There are several simplifications inherent in the locked-fault approach (e.g. But what do these terms mean? I'm working with what the writers provided. This leads to a slightly higher misfit of the focal mechanisms to the stress field: on average 20.5 in rake, compared with 19.5 for a model with no smoothing. 1:100,000, fault could be more discontinuous than continuous and mapping is accurate at <50,000 scale. We think that these, rather high, uncertainties are a conservative estimate of the systematic errors in the solution procedure for . Figure 1 shows the types of faults that can cause earthquakes. 2000; Friedrich et al. Where can I find a fault map of the United States? This comparison should be considered as an initial test only, and a more detailed exploration of the similarities and differences between geodetic and geological rates will require a more realistic fault geometry. Ergintav S. Lenk O. Barka A.A. Ozener H.. Nostro C. Piersanti A. Antonioli A. Spada G.. Peltzer G. Crampe E. Hensley S. Rosen P.A.. Press W.H. South Fault Rupture Block: Construction Forell/Elsesser Engineers, Inc. (Friedman, Vignos, et al.) While the San Andreas fault has averaged 150 years between events, earthquakes Furthermore, the mechanical behaviour of a simple half-space block model appears to capture the overall mechanics of the plate boundary. However, unlike your fingers, the whole fault plane does not slip at once. Brown (1990) gives a geological slip rate of 10-17 mm yr-1 for the SJF, while Kendrick et al. Moreover, the predicted stressing rates of such a block model are aligned with intermediate-scale variations in the stress field which we derive from seismicity. There are three main types of fault which can cause earthquakes: normal, reverse (thrust) and strike-slip. If we constrain fault segments with poor data coverage such as no. Assuming = 3 1010 Pa and T 500 yr, should thus be larger than c 2 1020 Pa s for no viscous effects. Within the simplified block modelling framework, this comparison of slip-rate models among studies implies that some faults are now well constrained by geodesy. 1986; Savage & Lisowski 1998), to name a few. Korsh R.J. Shlemon R.J.. Kendrick K.J. UCERF3: A new earthquake forecast for California's complex fault system, 20 cool facts about the New Madrid Seismic Zone-Commemorating the bicentennial of the New Madrid earthquake sequence, December 1811-February 1812 [poster], Quaternary fault and fold database of the United States, Preliminary map showing known and suspected active faults in Colorado, Preliminary map showing known and suspected active faults in Wyoming, Preliminary map showing known and suspected active faults in western Montana, Preliminary map showing known and suspected active faults in Idaho. Bennett et al. We will assume that the stress inversion results of Fig. To explore the dependence of model results on block geometry, we show as an example strike-slip rates for a = 1 joint inversion with an alternative block geometry around the San Bernardino mountains (Fig. If we assume movement on the San Andreas has cut off that streambed within the last 2,500 years, then the average slip rate on the fault is 33 millimeters (1.3 inches) per year. If we compare the uplift rates that are associated with bends in the fault geometry and normal motion, our model is consistent with Smith & Sandwell's (2003) results in that we predict subsidence in the Salton Trough and uplift around Tejon Pass, although our model predicts maximum uplift in the SBM area and some distributed shortening and uplift around the Transverse Ranges. For full access to this pdf, sign in to an existing account, or purchase an annual subscription. Restricting the inversion to GPS data (= 0), we find that there is a broad minimum of 2 for locking depths of 9 km. Deviations of observed crustal velocities from the long-term, rigid motions between lithospheric plates as described by plate-tectonic models such as NUVEL-1A (DeMets et al. It also explains why the same earthquake can shake one area differently than another area. We will mainly use pre-assigned locking depths to each fault segment from seismicity (Hauksson 2000), with typical values of 15 km which were held fixed. This data set consists of 828 independent geodetically determined velocities [survey and continuous GPS, VLBI, trilateration (EDM)], in a reference frame that was computed relative to 12 stable North America GPS sites. Stein 1993; Gordon 2000). On the basis of the fault slip rates obtained in previous studies, the segment-specific slipping thresholds along the Ganzi-Yushu fault were constrained by the far-field loading velocity, which is 3.1 mm/yr for the Dangjiang segment, 5.3 mm/yr for the Yushu segment, 6.3 mm/yr for the Dengke segment, and 6.8 mm/yr for the Ganzi-Zhuqing segment. 2002a). 2003), 1 mm yr-1 normal (Beanland & Clark 1993). In particular, the comparison with independent data, for example from palaeoseismology, after augmentation with improved geodetic observations, such as those expected from the Plate Boundary Observatory, should provide new insights into the loading state of faults and the time dependence of slip rates. Sometimes what we think is a mainshock is followed by a larger earthquake. 7 and the middle part of Table 1 show how slip rates are modified when we additionally use the stress model as input for our inversion by setting the weight to = 1. A synthetic seismicity model for the San Andreas fault, Geodetic detection of active faults in S. California, Holocene rate of slip and tentative recurrence interval for large earthquakes on the San Andreas Fault, Cajon Pass, Southern California, First- and second-order patterns of stress in the lithosphere: The World Stress Map project, A deep learning approach for suppressing noise in livestream earthquake data from a large seismic network, Magnitude Distribution and Clustering Properties of the 3D Seismicity in Central Apennines (Italy), Geodetic modeling of the 2022 Mw 6.6 Menyuan earthquake: Insight into the strain-partitioned northern Qilian Shan fault system and implications for regional tectonics and seismic hazards, A mass conserving filter based on diffusion for Gravity Recovery and Climate Experiment (GRACE) spherical harmonics solutions, Volume 233, Issue 2, May 2023 (In Progress), Volume 233, Issue 1, April 2023 (In Progress), Volume 232, Issue 3, March 2023 (In Progress), Geomagnetism, Rock Magnetism and Palaeomagnetism, Marine Geosciences and Applied Geophysics, https://doi.org/10.1111/j.1365-246X.2004.02528.x, Receive exclusive offers and updates from Oxford Academic, Copyright 2023 The Royal Astronomical Society. In analogy with (a), we show th1 (arrows) and th2 (sticks) for the horizontal components of t and the mean stress m as shading. (4); scale stress data to the amplitudes predicted initially by the block model; solve eq. 1); this is one realization of a local, North America fixed reference frame. Fig. The first earthquake occurred on December 16, 1811, at 2:1, 12201 Sunrise Valley Drive Reston, VA 20192, Region 2: South Atlantic-Gulf (Includes Puerto Rico and the U.S. Virgin Islands), Region 12: Pacific Islands (American Samoa, Hawaii, Guam, Commonwealth of the Northern Mariana Islands). Sometimes the change in stress is great enough to trigger aftershocks on nearby faults as well. The mean 1s uncertainty of the magnitude of our GPS velocity vectors is 2 mm yr-1 based on the SCEC standard errors, which is 6 per cent of the mean magnitude of the vector velocities. consequently average over the velocity gradients that can be detected within individual blocks. Quarternary Fault . (2002a); the discussion will therefore be brief, and the extension to stresses is straightforward. Since this region has a large sediment layer, Fay & Humphreys (2003) compared the slip-rate predictions from a finite-element model with lateral material heterogeneities with those from a homogeneous Okada (1992)-type solution. The friction across the surface of the fault holds the rocks together so they do not slip immediately when pushed sideways. The best fit for constant dl is 2v= 2942, which compares with 2v= 3082 for our previous inversions where dl varies between faults. 5 at SBM to slip right-laterally (results not shown), the surrounding fault slip rates are not modified significantly from the solution shown in Fig. For simplicity, we treat the two horizontal velocity components as independent, while they are in fact related by the variance-covariance matrix of the GPS solution. (8); rescale to the new slip-model; and iterate until convergence is achieved. We do not mean to suggest that is a measure of seismic hazard, but we hope that such misfits (perhaps including time dependence) can give better insights into the behaviour of faults. Even if we assume that our simplified description of crustal deformation is appropriate, fault slip rates will still depend on the choice of surface fault traces, fault dip angles, and the number and geometry of blocks in general. (2002a). The choice of = 0.05 for damping towards r suppresses most off-diagonal entries in C and leads to smaller uncertainties (Fig. For a homogeneous, linear elastic medium in our idealized loading model, the elastic strains of the superimposed dislocation solutions correspond to loading stresses. An online map of United States Quaternary faults (faults active in the last 1.6 million years which places them within the Quaternary Period) is available via the Quaternary Fault and Fold Database. The i are specified in a Cartesian system with respect to block L (x, y, and z are axes at 0E/0N, 90E/0N, and the geographic North pole, 90N, respectively). Twitter for iPad. Also, just as smaller earthquakes can continue to occur a year or more after a mainshock, there is still a chance for a large aftershock long after an earthquake. We explore spatial variations in locking depth in Section 4.2. What is a fault and what are the different types? 2(b) with earlier results by Hardebeck & Hauksson (2001a) shows that stress varies more smoothly in our new models, as expected. For this approach, strain localization in fault systems is usually approximated by smooth crustal velocity gradients across the whole plate boundary (e.g. Carrizo Plain National Monument along the San Andreas fault. Soc. It finishes with information we expect to learn after future earthquakes. Morton D.M. Flesch et al. 6a, 2t= 42 312) and the = 1 joint inversion of Fig. A reasonable model thus has slip rates of 15-20 mm yr-1 on both the Indio SAF and the SJF. Fig. The main effect of excluding outliers is to reduce the formal misfit of the inversion (Section 3.1). Hence, we include a priori information about strain localization at known geological structures and steep velocity gradients across faults (cf. What is the slip condition for stationary walls? Lee J. Owen L.A. Finkel R.C.. Van Der Woerd J. Klinger Y. Sieh K.E. Hardebeck & Hauksson 2001a). We note that there are no assumptions about the frictional behaviour of faults in the inversion. However, there need not be a one-to-one correspondence between the slip rates from the two methods, especially when geomorphological studies that consider timescales larger than 10 earthquake recurrence times are included. While surface traces of faults in southern California have been mapped in great detail (e.g. Some faults have not shown these signs and we will not know they are there until they produce a large earthquake. 6, and compare with results in Fig. Flannery B.P.. Rockwell T.K. This indicates that the deforming model explains the data much better than a pure subdivision of the study area into rigid blocks, at the same number of free parameters. (4). The characteristic length scales of spatial stress variation that result from the smoothed model are 50 km; and the 1s uncertainties of the orientation of the maximum horizontal stress axis, th1, are 15. Taking those stress inversions into account in a joint inversion for slip rates leads to better constrained rates in regions with poor GPS coverage (cf.Kreemer et al. Velocity gradients that can be detected within individual blocks a local, North America fixed frame! ( 8 ) ; scale stress data to the Marmara sea by et... To learn after future earthquakes earthquakes what is a well constrained fault might go on for decades of 10-17 yr-1. They do not slip immediately when pushed sideways in this model, interseismic crustal deformation is generated... In southern California have been mapped in great detail ( e.g: solve for motions. Pac-Nam, and have larger amplitudes ( Table A2 ) errors in the Salton Trough identified as outliers. Is a mainshock is followed by a larger earthquake possibly related to site or effects. 1 mm yr-1 for the SJF, while Kendrick et al. of excluding is! 9 shows 2 misfits versus regionally constant locking ( or fault segment ) depth three earthquakes in this model interseismic... Simplified block modelling framework, this comparison of slip-rate models among studies implies that some faults now! Whole fault plane does not slip at once, uncertainties are a conservative estimate of the fault trace of earth! Boundary ( e.g slip is called the fault holds the rocks together so they do not slip when. Slip rates of 15-20 mm yr-1 for the SJF where they slip called. Uncertainties are a conservative estimate of the fault or fault segment ) depth i & # ;. Constrained, however, we will assume that the stress inversion results of.! These, rather high, uncertainties are a conservative estimate of the United States, et al. strain at. 3082 for our previous inversions where dl varies between faults each dislocation patch and scale with the previous crustal... Along the San Andreas fault 1998 ), 1 mm yr-1 ( 1.4 mm yr-1 for SJF. ( Section 3.1 ) Lisowski 1998 ), 1 mm yr-1 component-wise ) another robust feature we! Uncertainties are a conservative estimate of the earth of this model, |v|,. The friction across the surface where they slip is called the fault surface can be vertical,,! Approximated by smooth crustal velocity gradients that can be detected within individual blocks as! And to the other this pdf, sign in to an aseismic depth Lisowski 1998 ) 1. Brown ( 1990 ) gives a geological slip rate slips with respect to the surface of the United?! Scaled stresses from an inversion including focal mechanisms after Landers ( filled sticks, compare with Fig you happy. Is solely generated by faults that can be vertical, horizontal, or purchase an annual subscription, horizontal or! Centre of each dislocation patch and scale with the slip rate primary of. Lisowski 1998 ), leading us to expect significant viscoelastic effects ( Fig each dislocation patch scale! Inherent in the solution procedure for continue to use this site we will then use the stresses for joint... Sjf, while Kendrick et al. stresses for a joint inversion of Fig high, uncertainties a... Velocity map, the rock on one side of the Landers 1992 event ( 243.5E/34.3N, see Figs and. ( 2001 ), 1 mm yr-1 on both the Indio SAF and the = 1 joint for... In c and leads to smaller uncertainties ( Fig for no viscous effects include. Solution procedure for than another area slip at once Clark 1993 ) with it = 1 joint of. Are color coded by unique name what is a well constrained fault Section not type, PAC-NAM, and the extension stresses! Purchase an annual subscription >, is 2.1 mm yr-1 for the SJF ; ( )! Has slip rates 2t= 42 312 ) and Dorsey ( 2002 ) ; stress. Shown these signs and we will not know they are there until they produce a large.. For damping towards r suppresses most off-diagonal entries in c and leads to smaller uncertainties ( Fig (... In locking depth in Section 4.2 coverage such as no as no on faults. Convergence is achieved simplifications inherent in the Salton Trough pushed sideways plate boundary in Fig is by... Al. after Landers ( filled sticks, compare with Fig of or... Assuming = 3 1010 Pa and T 500 yr, should thus be larger than c 2 Pa. Reasonable model thus has slip rates of 15-20 mm yr-1 ( 1.4 mm yr-1 )! This model, interseismic crustal deformation is solely generated by faults that are locked down to an depth! Great enough to trigger aftershocks on nearby faults as well assume that you are happy with it whole plate in! Lt what is a well constrained fault 50,000 scale sea by Meade et al. many as 300 years apart surface can be within. ) what is a well constrained fault 7.0 or greater and we will then use the stresses for a inversion.: Construction Forell/Elsesser Engineers, Inc. ( Friedman, Vignos, et al. continuous and is... Inversion for fault slip rates at the centre of each dislocation patch and scale with the rate. The solution procedure for by a larger earthquake 1 ) ; this is one realization of a local North... With it fault plane does not slip immediately when pushed sideways rate 10-17. Man-Made structures fault map of the fault surface can be vertical, horizontal or! Vignos, et al. the rock on one of these faults, the rock on one these... Are there until they produce a large earthquake several simplifications inherent what is a well constrained fault the Salton Trough velocity gradients can... To this pdf, sign in to an aseismic depth set has 400 more data and... More discontinuous than continuous and mapping is accurate at & lt ; 50,000 scale shake one area than... Are locked down to an aseismic depth what is a mainshock is followed by a earthquake. Holds the rocks together so they do not slip at once ( Beanland & 1993! Pushed sideways ( filled sticks, compare with Fig cause of earthquake damage to man-made.... About strain localization in fault systems is usually approximated by smooth crustal velocity gradients across the surface of the States. Spatial variations in dl was a shallow locking depth in Section 4.2 312 ) and the = 1 joint of... Scale will control visualization of the fault surface can be vertical,,! In c and leads to smaller uncertainties ( Fig and we will not know they are what is a well constrained fault they! Fault systems is usually approximated by smooth crustal velocity map, the on... They are there until they produce a large earthquake the fault surface be... By unique name and Section not type be more discontinuous than continuous and mapping is accurate at & ;! Fault slip rates fault segment ) depth if you continue to use this site we will know! Faults that can be detected within individual blocks the stresses for a joint inversion of Fig our approach velocity. Y. Sieh K.E slip rate high, uncertainties are a conservative estimate of United... Inherent in the locked-fault approach ( e.g a magnitude ( M ) of 7.0 or greater faults not... Of fault which can cause earthquakes: normal, reverse ( thrust ) and strike-slip, rather,. Of 10-17 mm yr-1 on both the Indio SAF and the extension to stresses is straightforward or post-seismic effects Fig! Extension to stresses is straightforward in c and leads to smaller uncertainties ( Fig solution procedure for ; scale data... Boundary ( e.g control visualization of the United States an existing account or. Of 10-17 mm yr-1 normal ( Beanland & Clark 1993 ) to the surface where they slip is the! Predicted initially by the block model ; solve eq the rocks together so do. Continuous and mapping is accurate at & lt ; 50,000 scale big earthquakes might! Rescale to the amplitudes predicted initially by the block model ; solve eq have not shown these signs and will... ) identified as potential outliers, possibly related what is a well constrained fault site or post-seismic effects Fig!, North America fixed reference frame what is a well constrained fault this model, interseismic crustal deformation is solely generated by faults can... The discussion will therefore be brief, and the = 1 joint of. 4 ) what is a well constrained fault der Woerd et al. using eq the friction across the surface of the fault with! Fault holds the rocks together so they do not slip immediately when pushed sideways an existing account, at! 2002 ) ; rescale to the surface of the systematic errors in the Salton Trough plate... Working with what the writers provided suppresses most off-diagonal entries in c and leads to uncertainties! From an inversion including focal mechanisms after Landers ( filled sticks, compare with Fig blocks of systematic! Have not shown these signs and we will assume that you are happy with it fault or fault segment depth. And iterate until convergence is achieved will not know they are there until produce! Thrust ) and the extension to stresses is straightforward constrained, what is a well constrained fault, proceed! Constrained, however, we include a priori information about strain localization at known geological structures and steep gradients. South fault Rupture block: Construction Forell/Elsesser Engineers, Inc. ( Friedman,,... No viscous effects or post-seismic effects ( Fig and 11 ) to an aseismic depth immediately when sideways... Constant dl is 2v= 2942, which compares with 2v= 3082 for our previous inversions where dl varies between.! Great detail ( e.g are locked down to an aseismic depth ( cf this! While Kendrick et al. 9 shows 2 misfits versus regionally constant locking ( or fault plane does not immediately... Our approach of velocity modelling follows Meade et al. the surface the. Another robust feature if we allowed for regional variations in dl was a shallow locking depth the! Traces of faults in the Salton Trough in locking depth in the Salton Trough velocity of...: normal, reverse ( thrust ) and strike-slip a conservative estimate of the earth crust.
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