A comparison of creepmeter records from nine sites along a 12-km segment of the Calaveras fault near Hollister, California and long-baseline strain changes for nine lines in the Hollister multiwavelength distance-measuring (MWDM) array has established that episodes of large-scale deformation both preceded and accompanied periods of creep activity monitored along the fault trace during 1976. A concept of episodic, deep-seated aseismic slip that contributes to loading and subsequent aseismic failure of shallow parts of the fault plane seems attractive, implying that the character of aseismic slip sensed along the surface trace may be restricted to a relatively shallow (~ 1-km) region on the fault plane. Preliminary results from simple dislocation models designed to test the concept demonstrate that extending the time-histories and amplitudes of creep events sensed along the fault trace to depths of up to 10 km on the fault plane cannot simulate adequately the character and amplitudes of large-scale episodic movements observed at points more than 1 km from the fault. Properties of a 2–3-km-thick layer of unconsolidated sediments present in Hollister Valley, combined with an essentially rigid-block behavior in buried basement blocks, might be employed in the formulation of more appropriate models that could predict patterns of shallow fault creep and large-scale displacements much more like those actually observed.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90263-4","issn":"00401951","usgsCitation":"Slater, L., and Burford, R.O., 1979, A comparison of long-baseline strain data and fault creep records obtained near Hollister, California: Tectonophysics, v. 52, no. 1-4, p. 481-496, https://doi.org/10.1016/0040-1951(79)90263-4.","productDescription":"16 p.","startPage":"481","endPage":"496","costCenters":[],"links":[{"id":222266,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Hollister","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.63417354009724,\n 37.03514059462465\n ],\n [\n -121.63417354009724,\n 36.70425231730185\n ],\n [\n -121.22588991098016,\n 36.70425231730185\n ],\n [\n -121.22588991098016,\n 37.03514059462465\n ],\n [\n -121.63417354009724,\n 37.03514059462465\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e36ce4b0c8380cd45fe1","contributors":{"authors":[{"text":"Slater, L.E.","contributorId":35063,"corporation":false,"usgs":true,"family":"Slater","given":"L.E.","email":"","affiliations":[],"preferred":false,"id":364024,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Burford, Robert O.","contributorId":52560,"corporation":false,"usgs":true,"family":"Burford","given":"Robert","middleInitial":"O.","affiliations":[],"preferred":false,"id":364025,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70012504,"text":"70012504 - 1979 - Two areas of probable holocene deformation in southwestern Utah","interactions":[],"lastModifiedDate":"2025-09-04T16:18:27.471378","indexId":"70012504","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Two areas of probable holocene deformation in southwestern Utah","docAbstract":"Recent geologic studies in southwestern Utah indicate two areas of probable Holocene ground deformation.
1. (1) A narrow arm of Lake Bonneville is known to have extended southward into Escalante Valley as far as Lund, Utah. Remnants of weakly developed shoreline features, which we have recently found, suggest that Lake Bonnevile covered an area of about 800 km2 beyond its previously recognized limits near Lund. Shoreline elevations show a gradual increase from 1553 m near Lund to 1584 m at a point 50 km further southwest, representing a reversal of the pattern that would result from isostatic rebound. The conspicuously flat floor of Escalante Valley covers an additional 100 km2 southward toward Enterprise, where its elevation is greater than 1610 m, but no shoreline features are recognizable; therefore, the former presence of the lake is only suspected. The measured 31-m rise over 50 km and the suspected 57-m rise in elevation over 70 km apparently occurred after Lake Bonnevile abandoned this area. The abandonment could have occurred as recently as 13,000 years ago, in which case the uplift is mainly of Holocene age. It probably has a deep-seated tectonic origin because it is situated above an inferred 9-km upwarp of the mantle that has been reported beneath the southern part of Escalante Valley on the basis of teleseismic P-wave residuals.
2. (2) Numerous closed topographic basins, ranging from a few hundred square meters to 1 km2 in area, are found at various elevations along the west margin of the Colorado Plateau northeast of Cedar City. Geologic mapping in that area indicates that the basins are located over complex structural depressions in which the rocks are faulted and folded. Several of the depressions are perched along the walls of the West Fork of Braffits Creek, one of a few north-draining creeks that have incised deeply into the plateau margin. Extremely active modern erosion by the creek has produced a 6-km-long gorge along which excellent exposures provide good evidence that the topographic depressions, as well as the entire valley, are located over a north-trending structural graben in which rocks of Cretaceous, Tertiary, and Quaternary age are complexly deformed. The trough appears to be actively subsiding, as evidenced by inward-dipping youthful scarps and V-shaped trenches found along both walls of the valley. The scarp on the east side is continuous for 1.5 km, and that on the west is discontinuous for the same distance. Charcoal-bearing alluvium from a sequence of faulted sedimentary debris in the inner gorge has yielded discordant dates by the 14C technique, but the dates suggest that at least 6 m of fault displacement occurred during the Late Holocene.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90257-9","issn":"00401951","usgsCitation":"Anderson, R., and Bucknam, R., 1979, Two areas of probable holocene deformation in southwestern Utah: Tectonophysics, v. 52, no. 1-4, p. 417-430, https://doi.org/10.1016/0040-1951(79)90257-9.","productDescription":"14 p.","startPage":"417","endPage":"430","costCenters":[],"links":[{"id":222419,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Utah","otherGeospatial":"southwestern Utah","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -112.13988686177788,\n 38.76852920061029\n ],\n [\n -112.13988686177788,\n 36.95389428410948\n ],\n [\n -109.0304136471782,\n 36.95389428410948\n ],\n [\n -109.0304136471782,\n 38.76852920061029\n ],\n [\n -112.13988686177788,\n 38.76852920061029\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb94be4b08c986b327baf","contributors":{"authors":[{"text":"Anderson, R.E.","contributorId":91479,"corporation":false,"usgs":true,"family":"Anderson","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":363772,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bucknam, R.C.","contributorId":35744,"corporation":false,"usgs":true,"family":"Bucknam","given":"R.C.","affiliations":[],"preferred":false,"id":363771,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70012441,"text":"70012441 - 1979 - Evidence for the recurrence of large-magnitude earthquakes along the Makran coast of Iran and Pakistan","interactions":[],"lastModifiedDate":"2025-09-04T15:52:06.302636","indexId":"70012441","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Evidence for the recurrence of large-magnitude earthquakes along the Makran coast of Iran and Pakistan","docAbstract":"The presence of raised beaches and marine terraces along the Makran coast indicates episodic uplift of the continental margin resulting from large-magnitude earthquakes. The uplift occurs as incremental steps similar in height to the 1–3 m of measured uplift resulting from the November 28, 1945 (M 8.3) earthquake at Pasni and Ormara, Pakistan. The data support an E—W-trending, active subduction zone off the Makran coast.
The raised beaches and wave-cut terraces along the Makran coast are extensive with some terraces 1–2 km wide, 10–15 m long and up to 500 m in elevation. The terraces are generally capped with shelly sandstones 0.5–5 m thick. Wave-cut cliffs, notches, and associated boulder breccia and swash troughs are locally preserved. Raised Holocene accretion beaches, lagoonal deposits, and tombolos are found up to 10 m in elevation. The number and elevation of raised wave-cut terraces along the Makran coast increase eastward from one at Jask, the entrance to the Persian Gulf, at a few meters elevation, to nine at Konarak, 250 km to the east. Multiple terraces are found on the prominent headlands as far east as Karachi. The wave-cut terraces are locally tilted and cut by faults with a few meters of displacement.
Long-term, average rates of uplift were calculated from present elevation, estimated elevation at time of deposition, and 14C and U–Th dates obtained on shells. Uplift rates in centimeters per year at various locations from west to east are as follows: Jask, 0 (post-Sangamon); Konarak, 0.031–0.2 (Holocene), 0.01 (post-Sangamon); Ormara 0.2 (Holocene).
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90269-5","issn":"00401951","usgsCitation":"Page, W., Alt, J.N., Cluff, L., and Plafker, G., 1979, Evidence for the recurrence of large-magnitude earthquakes along the Makran coast of Iran and Pakistan: Tectonophysics, v. 52, no. 1-4, p. 533-547, https://doi.org/10.1016/0040-1951(79)90269-5.","productDescription":"15 p.","startPage":"533","endPage":"547","costCenters":[],"links":[{"id":222351,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Iran, Pakistan","otherGeospatial":"Makran coast","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n 56.93988761081735,\n 26.31424458821168\n ],\n [\n 56.93988761081735,\n 20.70437454508202\n ],\n [\n 72.46275584520896,\n 20.70437454508202\n ],\n [\n 72.46275584520896,\n 26.31424458821168\n ],\n [\n 56.93988761081735,\n 26.31424458821168\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0d55e4b0c8380cd52f67","contributors":{"authors":[{"text":"Page, W.D.","contributorId":52725,"corporation":false,"usgs":true,"family":"Page","given":"W.D.","email":"","affiliations":[],"preferred":false,"id":363590,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Alt, J. N.","contributorId":44667,"corporation":false,"usgs":true,"family":"Alt","given":"J.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":363589,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cluff, L.S.","contributorId":93902,"corporation":false,"usgs":true,"family":"Cluff","given":"L.S.","email":"","affiliations":[],"preferred":false,"id":363591,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Plafker, George 0000-0003-3972-0390","orcid":"https://orcid.org/0000-0003-3972-0390","contributorId":36603,"corporation":false,"usgs":true,"family":"Plafker","given":"George","affiliations":[],"preferred":false,"id":363588,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70010323,"text":"70010323 - 1979 - Dislocation modeling of creep-related tilt changes","interactions":[],"lastModifiedDate":"2025-09-04T16:00:42.765558","indexId":"70010323","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Dislocation modeling of creep-related tilt changes","docAbstract":"A marked change is observed in P/SV amplitude ratios, measured at station TPC, from foreshocks to aftershocks of the Galway Lake earthquake. This change is interpreted to be the result of a change in fault-plane orientation occurring between foreshocks and aftershocks.
The Galway Lake earthquake, ML= 5.2, occurred on June 1, 1975. The first-motion fault-plane solutions for the main shock and most foreshocks and aftershocks indicate chiefly right-lateral strike-slip on NNW-striking planes that dip steeply, 70–90°, to the WSW. The main event was preceded by nine located foreshocks, ranging in magnitude from 1.9 to 3.4, over a period of 12 weeks, starting on March 9, 1975. All of the foreshocks form a tight cluster approximately 1 km in diameter. This cluster includes the main shock. Aftershocks are distributed over a 6-km-long fault zone, but only those that occurred inside the foreshock cluster are used in this study.
Seismograms recorded at TPC (Δ = 61 km), PEC (Δ = 93 km), and CSP (Δ = 83 km) are the data used here. The seismograms recorded at TPC show very consistent P/SV amplitude ratios for foreshocks. For aftershocks the P/SV ratios are scattered, but generally quite different from foreshock ratios. Most of the scatter for the aftershocks is confined to the two days following the main shock. Thereafter, however, the P/SV ratios are consistently half as large as for foreshocks. More subtle (and questionable) changes in the P/SV ratios are observed at PEC and CSP.
Using theoretical P/SV amplitude ratios, one can reproduce the observations at TPC, PEC and CSP by invoking a 5–12° counterclockwise change in fault strike between foreshocks and aftershocks. This interpretation is not unique, but it fits the data better than invoking, for example, changes in dip or slip angle. First-motion data cannot resolve this small change, but they permit it. Attenuation changes would appear to be ruled out by the fact that changes in the amplitude ratios, PTPC/PPEC and ptpc/pcsp, are observed, and these changes accompany the changes in P/SV.
Observations for the Galway Lake earthquake are similar to observations for the Oroville, California, earthquake (ML = 5.7) of August 1, 1975, and the Brianes Hills, California, earthquake (ML = 4.3) of January 8, 1977 (Lindh et al., Science Vol. 201, pp. 56–59).
A change in fault-plane orientation between foreshocks and aftershocks may be understandable in terms of early en-echelon cracking (foreshocks) giving way to shear on the main fault plane (main shock plus aftershocks). Recent laboratory data (Byerlee et al., Tectonophysics, Vol. 44, pp. 161–171) tend to support this view.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90276-2","issn":"00401951","usgsCitation":"Fuis, G., and Lindh, A., 1979, A change in fault-plane orientation between foreshocks and aftershocks of the Galway Lake earthquake, ML = 5.2, 1975, Mojave Desert, California: Tectonophysics, v. 52, no. 1-4, p. 601-602, https://doi.org/10.1016/0040-1951(79)90276-2.","productDescription":"2 p.","startPage":"601","endPage":"602","costCenters":[],"links":[{"id":221820,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Mojave Desert","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.88041412845288,\n 35.57353922357994\n ],\n [\n -116.88041412845288,\n 34.066603856422134\n ],\n [\n -114.86128184613081,\n 34.066603856422134\n ],\n [\n -114.86128184613081,\n 35.57353922357994\n ],\n [\n -116.88041412845288,\n 35.57353922357994\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e33ee4b0c8380cd45ed8","contributors":{"authors":[{"text":"Fuis, G. S.","contributorId":83131,"corporation":false,"usgs":true,"family":"Fuis","given":"G. S.","affiliations":[],"preferred":false,"id":363473,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lindh, A.G.","contributorId":24784,"corporation":false,"usgs":true,"family":"Lindh","given":"A.G.","email":"","affiliations":[],"preferred":false,"id":363472,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010362,"text":"70010362 - 1979 - Elastic expansion of the lithosphere caused by groundwater withdrawal in south-central Arizona","interactions":[],"lastModifiedDate":"2025-09-04T16:51:35.160881","indexId":"70010362","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Elastic expansion of the lithosphere caused by groundwater withdrawal in south-central Arizona","docAbstract":"Relative crustal uplift observed from 1948–1949 to 1967 in the Lower Santa Cruz River Basin in south-central Arizona is attributed at least in part to elastic expansion of the lithosphere induced by the removal, and subsequent loss by evapo transpiration, of 4.35 × 1013 kg of groundwater from alluvium. The area of unloading is approximately 8070 km2. Uplift, relative to an apparently stable area west of the unloaded area, was observed in two areas near Casa Grande and Florence where crystalline bedrock is either close to the land surface or crops out through alluvium from which groundwater was withdrawn. The magnitudes of uplift were approximately 6.3 and 7.5 cm respectively. The observations are based on first-order leveling. The observations are significant at three standard deviations for random surveying errors, and are not believed to be affected by systematic errors. However, the 7.5-cm uplift observed at Florence may be from 1 to 2 cm in excess of the actual uplift because of the possibility of subsidence of a tie point due to groundwater pumping during the leveling in 1948–1949.
Uplift is attributed to groundwater withdrawal on three bases. First, the observed uplift is consistent with a theoretical evaluation of elastic expansion based on linear elasticity theory. For the observed distribution of unloading and uplift and a Poisson's ratio of 0.25, a Young's modulus for the lithosphere of approximately 0.68 Mbar is implied. This value is comparable to values of the lithosphere reported elsewhere. Second, the magnitude of uplift compares favorably with the magnitude of elastic depression caused by the formation of Lake Mead, Arizona—Nevada, 430 km northwest of the study area, when allowance is made for the different magnitudes and areal distributions of surface (un)loading. And third, in the area near Casa Grande, a reversal in the sense of bedrock displacement form subsidence of tectonic origin to uplift approximately coincided with the beginning of large groundwater overdraft. The uplift from 1948 to 1967 near Casa Grande was preceded from 1905 to 1948 by 7–8 cm of tectonic subsidence; no precise data for the area near Florence are available before 1948.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90236-1","issn":"00401951","usgsCitation":"Holzer, T., 1979, Elastic expansion of the lithosphere caused by groundwater withdrawal in south-central Arizona: Tectonophysics, v. 52, no. 1-4, p. 304-304, https://doi.org/10.1016/0040-1951(79)90236-1.","productDescription":"1 p.","startPage":"304","endPage":"304","costCenters":[],"links":[{"id":219606,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona","otherGeospatial":"south-central Arizona","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -113.03416166288255,\n 33.907867445210215\n ],\n [\n -113.03416166288255,\n 31.331659801949186\n ],\n [\n -110.66198484870762,\n 31.331659801949186\n ],\n [\n -110.66198484870762,\n 33.907867445210215\n ],\n [\n -113.03416166288255,\n 33.907867445210215\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0881e4b0c8380cd51b4e","contributors":{"authors":[{"text":"Holzer, T.L.","contributorId":35739,"corporation":false,"usgs":true,"family":"Holzer","given":"T.L.","email":"","affiliations":[],"preferred":false,"id":358722,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010336,"text":"70010336 - 1979 - Fault-crossing P delays, epicentral biasing, and fault behavior in central California","interactions":[],"lastModifiedDate":"2025-09-04T15:38:24.9374","indexId":"70010336","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Fault-crossing P delays, epicentral biasing, and fault behavior in central California","docAbstract":"The P delays across the San Andreas fault zone in central California have been determined from travel-time differences at station pairs spanning the fault, using off-fault local earthquake or quarry blast sources. Systematic delays as large as 0.4 sec have been observed for paths crossing the fault at depths of 5-10 km. These delays can account for the apparent deviation of epicenters from the mapped fault trace. The largest delays occur along the San Andreas fault between San Juan Bautista and Bear Valley and Between Bitterwater Valley and Parkfield. Spatial variations in fault behavior correlate with the magnitude of the fault-crossing P delay. The delay decreases to the northwest of San Juan Bautista across the \"locked\" section of the San Andreas fault and also decreases to the southeast approaching Parkfield. Where the delay is large, seismicity is relatively high and the fault is creeping.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90275-0","issn":"00401951","usgsCitation":"Marks, S., and Bufe, C., 1979, Fault-crossing P delays, epicentral biasing, and fault behavior in central California: Tectonophysics, v. 52, no. 1-4, p. 600-600, https://doi.org/10.1016/0040-1951(79)90275-0.","productDescription":"1 p.","startPage":"600","endPage":"600","costCenters":[],"links":[{"id":218859,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"central California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.09843292088527,\n 36.5575453150701\n ],\n [\n -121.09843292088527,\n 35.76950556267637\n ],\n [\n -120.30334394341517,\n 35.76950556267637\n ],\n [\n -120.30334394341517,\n 36.5575453150701\n ],\n [\n -121.09843292088527,\n 36.5575453150701\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0f1fe4b0c8380cd5379f","contributors":{"authors":[{"text":"Marks, S.M.","contributorId":33687,"corporation":false,"usgs":true,"family":"Marks","given":"S.M.","email":"","affiliations":[],"preferred":false,"id":358664,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bufe, C. G.","contributorId":79443,"corporation":false,"usgs":true,"family":"Bufe","given":"C. G.","affiliations":[],"preferred":false,"id":358665,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010424,"text":"70010424 - 1979 - Quaternary crustal deformation along a major branch of the San Andreas fault in central California","interactions":[],"lastModifiedDate":"2025-09-04T16:47:46.74958","indexId":"70010424","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Quaternary crustal deformation along a major branch of the San Andreas fault in central California","docAbstract":"Deformed marine terraces and alluvial deposits record Quaternary crustal deformation along segments of a major, seismically active branch of the San Andreas fault which extends 190 km SSE roughly parallel to the California coastline from Bolinas Lagoon to the Point Sur area. Most of this complex fault zone lies offshore (mapped by others using acoustical techniques), but a 4-km segment (Seal Cove fault) near Half Moon Bay and a 26-km segment (San Gregorio fault) between San Gregorio and Point Ano Nuevo lie onshore.
At Half Moon Bay, right-lateral slip and N—S horizontal compression are expressed by a broad, synclinal warp in the first (lowest: 125 ka?) and second marine terraces on the NE side of the Seal Cove fault. This structure plunges to the west at an oblique angle into the fault plane. Linear, joint0controlled stream courses draining the coastal uplands are deflected toward the topographic depression along the synclinal axis where they emerge from the hills to cross the lowest terrace. Streams crossing the downwarped part of this terrace adjacent to Half Moon Bay are depositing alluvial fans, whereas streams crossing the uplifted southern limb of the syncline southwest of the bay are deeply incised. Minimum crustal shortening across this syncline parallel to the fault is 0.7% over the past 125 ka, based on deformation of the shoreline angle of the first terrace.
Between San Gregorio and Point Ano Nuevo the entire fault zone is 2.5–3.0 km wide and has three primary traces or zones of faulting consisting of numerous en-echelon and anastomozing secondary fault traces. Lateral discontinuities and variable deformation of well-preserved marine terrace sequences help define major structural blocks and document differential motions in this area and south to Santa Cruz. Vertical displacement occurs on all of the fault traces, but is small compared to horizontal displacement. Some blocks within the fault zone are intensely faulted and steeply tilted. One major block 0.8 km wide east of Point Ano Nuevo is downdropped as much as 20 m between two primary traces to form a graben presently filling with Holocene deposits. Where exposed in the sea cliff, these deposits are folded into a vertical attitude adjacent to the fault plane forming the south-west margin of the graben. Near Point Ano Nuevo sedimentary deposits and fault rubble beneath a secondary high-angle reverse fault record three and possibly six distinct offset events in the past 125 ka.
The three primary fault traces offset in a right-lateral sense the shoreline angles of the two lowest terraces east of Point Ano Nuevo. The rates of displacement on the three traces are similar. The average rate of horizontal offset across the entire zone is between 0.63 and 1.30 cm/yr, based on an amino-acid age estimate of 125 ka for the first terrace, and a reasonable guess of 200–400 ka for the second terrace. Rates of this magnitude make up a significant part of the deficit between long-term relative plate motions (estimated by others to be about 6 cm/yr) and present displacement rates along other parts of the San Andreas fault system (about 3.2 cm/yr).
Northwestward tilt and convergence of six marine terraces northeast of Ano Nuevo (southwest side of the fault zone) indicate continuous gentle warping associated with right-lateral displacement since early or middle Pleistocene time. Minimum local crustal shortening of this block parallel to the fault is 0.2% based on tilt of the highest terrace. Five major, evenly spaced terraces southeast of Ano Nuevo on the southwest flank of Mt. Ben Lomond (northeast side of the fault zone) rise to an elevation of 240 m, indicating relatively constant uplift (about 0.19 m/ka and southwestward tilt since Early or Middle Pleistocene time (Bradley and Griggs, 1976).
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90250-6","issn":"00401951","usgsCitation":"Weber, G.E., Lajoie, K.R., and Wehmiller, J., 1979, Quaternary crustal deformation along a major branch of the San Andreas fault in central California: Tectonophysics, v. 52, no. 1-4, p. 378-379, https://doi.org/10.1016/0040-1951(79)90250-6.","productDescription":"2 p.","startPage":"378","endPage":"379","costCenters":[],"links":[{"id":219530,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"central California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.5194629235352,\n 37.973169375002726\n ],\n [\n -120.05133073107262,\n 35.654205501747015\n ],\n [\n -118.17267019978546,\n 33.17708096559648\n ],\n [\n -117.02307974497106,\n 33.24006195557827\n ],\n [\n -120.19211617365147,\n 38.46789540600368\n ],\n [\n -121.5194629235352,\n 37.973169375002726\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a928ce4b0c8380cd8090a","contributors":{"authors":[{"text":"Weber, G. E.","contributorId":28612,"corporation":false,"usgs":true,"family":"Weber","given":"G.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":358885,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lajoie, K. R.","contributorId":6828,"corporation":false,"usgs":true,"family":"Lajoie","given":"K.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":358884,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wehmiller, J.F.","contributorId":37891,"corporation":false,"usgs":false,"family":"Wehmiller","given":"J.F.","email":"","affiliations":[],"preferred":false,"id":358886,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70010335,"text":"70010335 - 1979 - Earthquake recurrence on the Calaveras fault east of San Jose, California","interactions":[],"lastModifiedDate":"2025-09-03T16:51:14.982934","indexId":"70010335","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Earthquake recurrence on the Calaveras fault east of San Jose, California","docAbstract":"Occurrence of small (3 ⩽ ML < 4) earthquakes on two 10-km segments of the Calaveras fault between Calaveras and Anderson reservoirs follows a simple linear pattern of elastic strain accumulation and release. The centers of these independent patches of earthquake activity are 20 km apart. Each region is characterized by a constant rate of seismic slip as computed from earthquake magnitudes, and is assumed to be an isolated locked patch on a creeping fault surface. By calculating seismic slip rates and the amount of seismic slip since the time of the last significant (M ⩾ 3) earthquake, it is possible to estimate the most likely date of the next (M ⩾- 3) event on each patch. The larger the last significant event, the longer the time until the next one. The recurrence time also appears to be increased according to the moment of smaller (2 < ML < 3) events in the interim. The anticipated times of future larger events on each patch, on the basis of preliminary location data through May 1977 and estimates of interim activity, are tabulated below with standard errors. The occurrence time for the southern zone is based on eight recurrent events since 1969, the northern zone on only three. The 95% confidence limits can be estimated as twice the standard error of the projected least-squares line. Events of M ⩾ 3 should not occur in the specified zones at times outside these limits. The central region between the two zones was the locus of two events (M = 3.6, 3.3) on July 3, 1977. These events occurred prior to a window based on the three point, post-1969 slip-time line for the central region.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90277-4","issn":"00401951","usgsCitation":"Bufe, C.G., Harsh, P., and Burford, R.O., 1979, Earthquake recurrence on the Calaveras fault east of San Jose, California: Tectonophysics, v. 52, no. 1-4, p. 603-603, https://doi.org/10.1016/0040-1951(79)90277-4.","productDescription":"1 p.","startPage":"603","endPage":"603","costCenters":[],"links":[{"id":218792,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"San Jose","otherGeospatial":"Calaveras fault","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.86532830653152,\n 37.52332164696976\n ],\n [\n -121.86532830653152,\n 37.42278769737207\n ],\n [\n -121.73138190198938,\n 37.42278769737207\n ],\n [\n -121.73138190198938,\n 37.52332164696976\n ],\n [\n -121.86532830653152,\n 37.52332164696976\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a04ffe4b0c8380cd50bea","contributors":{"authors":[{"text":"Bufe, Charles G. cbufe@usgs.gov","contributorId":1621,"corporation":false,"usgs":true,"family":"Bufe","given":"Charles","email":"cbufe@usgs.gov","middleInitial":"G.","affiliations":[],"preferred":true,"id":358663,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Harsh, Philip W.","contributorId":18028,"corporation":false,"usgs":true,"family":"Harsh","given":"Philip W.","affiliations":[],"preferred":false,"id":358661,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Burford, Robert O.","contributorId":52560,"corporation":false,"usgs":true,"family":"Burford","given":"Robert","middleInitial":"O.","affiliations":[],"preferred":false,"id":358662,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70010425,"text":"70010425 - 1979 - Anomalously high uplift rates along the Ventura-Santa Barbara coast, California-tectonic implications","interactions":[],"lastModifiedDate":"2025-09-04T16:32:57.145646","indexId":"70010425","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Anomalously high uplift rates along the Ventura-Santa Barbara coast, California-tectonic implications","docAbstract":"The NW—SE trending segments of the California coastline from Point Arena to Point Conception (500 km) and from Los Angeles to San Diego (200 km) generally parallel major right-lateral strike-slip fault systems. Minor vertical crustal movements associated with the dominant horizontal displacements along these fault systems are recorded in local sedimentary basins and slightly deformed marine terraces. Typical maximum uplift rates during Late Quaternary time are about 0.3 m/ka, based on U-series ages of corals and amino-acid age estimates of fossil mollusks from the lowest emergent terraces.
In contrast, the E–W-trending segments of the California coastline between Point Conception and Los Angeles (200 km) parallel predominantly northward-dipping thrust and high-angle reverse faults of the western Transverse Ranges. Along this coast, marine terraces display significantly greater vertical deformation. Amino-acid age estimates of mollusks from elevated marine terraces along the Ventura—Santa Barbara coast imply anomalously high uplift rates of between 1 and 6 m/ka over the past 40 to 100 ka. The deduced rate of terrace uplift decreases from Ventura to Los Angeles, conforming with a similar trend observed by others in contemporary geodetic data.
The more rapid rates of terrace uplift in the western Transverse Ranges reflect N—S crustal shortening that is probably a local accommodation of the dominant right-lateral shear strain along coastal California.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90251-8","issn":"00401951","usgsCitation":"Wehmiller, J., Sarna-Wojcicki, A., Yerkes, R.F., and Lajoie, K.R., 1979, Anomalously high uplift rates along the Ventura-Santa Barbara coast, California-tectonic implications: Tectonophysics, v. 52, no. 1-4, p. 380-380, https://doi.org/10.1016/0040-1951(79)90251-8.","productDescription":"1 p.","startPage":"380","endPage":"380","costCenters":[],"links":[{"id":219531,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"California coast","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -119.85156598520446,\n 34.52923383591113\n ],\n [\n -119.86104975444009,\n 34.283397046118026\n ],\n [\n -117.46165613782087,\n 32.589689118350094\n ],\n [\n -117.0256771795831,\n 32.54173941788879\n ],\n [\n -117.49267799689852,\n 33.52507937313166\n ],\n [\n -118.64005092871375,\n 34.311052657200904\n ],\n [\n -119.85156598520446,\n 34.52923383591113\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059ec4ce4b0c8380cd491a8","contributors":{"authors":[{"text":"Wehmiller, J.F.","contributorId":37891,"corporation":false,"usgs":false,"family":"Wehmiller","given":"J.F.","email":"","affiliations":[],"preferred":false,"id":358889,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sarna-Wojcicki, A. 0000-0002-0244-9149","orcid":"https://orcid.org/0000-0002-0244-9149","contributorId":38750,"corporation":false,"usgs":true,"family":"Sarna-Wojcicki","given":"A.","affiliations":[],"preferred":false,"id":358890,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Yerkes, R. F.","contributorId":24754,"corporation":false,"usgs":true,"family":"Yerkes","given":"R.","middleInitial":"F.","affiliations":[],"preferred":false,"id":358888,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Lajoie, K. R.","contributorId":6828,"corporation":false,"usgs":true,"family":"Lajoie","given":"K.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":358887,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70012208,"text":"70012208 - 1979 - The petrogenesis and trace-element geochemistry of intermediate lavas from Humphreys Peak, San Francisco volcanic field, Arizona","interactions":[],"lastModifiedDate":"2025-09-02T16:33:40.599462","indexId":"70012208","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"The petrogenesis and trace-element geochemistry of intermediate lavas from Humphreys Peak, San Francisco volcanic field, Arizona","docAbstract":"The San Francisco Mountain lavas exposed in the upper portion of the southeast slope of Humphreys Peak are composed of three petrographically distinct types: (1) a lower series of hornblende pyroxene andesites; (2) a group of hypersthene dacites; and (3) an upper series of olivine andesites. These rocks have been shown to be related by crystallization differentiation through comparison of groundmass and bulk rock-chemical data.
The major and trace elements from rocks representative of the volcanic field form continuous trends, an indication of differentiation rather than separate and discrete magma sources.
Xenoliths found in the volcanic field are composed of the proper major and trace element contents to allow their extraction from a primary melt to form residual melts of more silicic lavas. The alkali olivine basalts, probably formed by partial melting of the mantle at a depth of 35-60 km, may well have differentiated to the alkali-rich highalumina basalts at depths of 15-35 km (the lower crust of the Colorado Plateau) by removal of olivine and clinopyroxene. Some of both lava types erupted periodically onto the surface while others continued to differentiate. Removal of plagioclase, with more minor amounts of olivine and pyroxenes (of less mafic composition than those above), from the high-alumina basalts eventually may have resulted in magmas similar in composition to the intermediate and more silicic rocks. The intermediate and silicic magmas contain hornblende and probably formed between 5 and 8 km. This places a minimum depth of penetration by the normal faults, such as the Mesa Butte fault, along which many silicic centers are aligned, at a depth of 5-8 km.
Because of the continuous linear trends of the chemical data and the repetition over the past 6 m.y. of most of the rock types, the mantle beneath this southwestern margin of the Colorado Plateau apparently has not changed significantly during the past 6 m.y., nor is it likely to be very heterogeneous.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90294-4","issn":"00401951","usgsCitation":"Wenrich-Verbeek, K., 1979, The petrogenesis and trace-element geochemistry of intermediate lavas from Humphreys Peak, San Francisco volcanic field, Arizona: Tectonophysics, v. 61, no. 1-3, p. 103-129, https://doi.org/10.1016/0040-1951(79)90294-4.","productDescription":"27 p.","startPage":"103","endPage":"129","costCenters":[],"links":[{"id":222341,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona","city":"Flagstaff","otherGeospatial":"San Francsico volcanic field","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -112.5188489662613,\n 35.827824601481694\n ],\n [\n -112.5188489662613,\n 35.20713008309407\n ],\n [\n -110.93800016874307,\n 35.20713008309407\n ],\n [\n -110.93800016874307,\n 35.827824601481694\n ],\n [\n -112.5188489662613,\n 35.827824601481694\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"61","issue":"1-3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bae8be4b08c986b32418a","contributors":{"authors":[{"text":"Wenrich-Verbeek, K.J.","contributorId":74134,"corporation":false,"usgs":true,"family":"Wenrich-Verbeek","given":"K.J.","affiliations":[],"preferred":false,"id":362993,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010397,"text":"70010397 - 1979 - Preliminary results from comparisons of redundant tiltmeters at three sites in central California","interactions":[],"lastModifiedDate":"2025-09-05T16:39:39.066305","indexId":"70010397","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Preliminary results from comparisons of redundant tiltmeters at three sites in central California","docAbstract":"First-order vertical level surveys (National Geodetic Survey) repeated between 1955 and 1975 suggest that modern vertical crustal movements have taken place in the Atlantic Coastal Plain between Charleston, South Carolina and Savannah, Georgia. The relative sense of these movements correlates with the sense of displacement of Tertiary strata on known geologic structures. Whereas regional dip of strata in most of the Atlantic Coastal Plain is southeasterly, the regional dip of Tertiary strata in this part of the Coastal Plain averages 2 m/km to the south or southwest. Positive structural features disturb this regional dip along a poorly defined zone, about 25 km wide, parallel to the coast between Savannah and Charleston. Structural relief on these features is as much as 20 m. Repeated level lines that cross the Atlantic Coastal Plain elsewhere generally show an increase in modern relative subsidence from west to east. However, in the Charleston—Savannah area, the amount of relative subsidence remains fairly constant or decreases from west to east across the structural highs. At two localities near Charleston, where Tertiary beds are offset by faults roughly on strike with one another, an abrupt break in a repeated level line occurs where the level line crosses the probable extensions of these faults. The average modern rates of relative uplift and subsidence (assuming they are constant) are compatible with rates noted throughout the Coastal Plain. Long-term extrapolation of modern rates appears unreasonable; episodic or oscillatory movements are much more likely.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90223-3","issn":"00401951","usgsCitation":"Lyttle, P.T., Gohn, G., Higgins, B., and Wright, D., 1979, Vertical crustal movements in the Charleston, South Carolina-Savannah, Georgia area: Tectonophysics, v. 52, no. 1-4, p. 183-189, https://doi.org/10.1016/0040-1951(79)90223-3.","productDescription":"7 p.","startPage":"183","endPage":"189","costCenters":[],"links":[{"id":221822,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Georgia, South Carolina","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -81.89939091011503,\n 33.56449440727431\n ],\n [\n -81.89939091011503,\n 31.94598797126214\n ],\n [\n -79.42308747915132,\n 31.94598797126214\n ],\n [\n -79.42308747915132,\n 33.56449440727431\n ],\n [\n -81.89939091011503,\n 33.56449440727431\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bc22fe4b08c986b32a9a2","contributors":{"authors":[{"text":"Lyttle, Peter T.","contributorId":244786,"corporation":false,"usgs":false,"family":"Lyttle","given":"Peter","email":"","middleInitial":"T.","affiliations":[{"id":7065,"text":"USGS emeritus","active":true,"usgs":false}],"preferred":false,"id":363478,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gohn, Gregory S. ggohn@usgs.gov","contributorId":147414,"corporation":false,"usgs":true,"family":"Gohn","given":"Gregory S.","email":"ggohn@usgs.gov","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":false,"id":363476,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Higgins, Brenda","contributorId":106106,"corporation":false,"usgs":true,"family":"Higgins","given":"Brenda","email":"","affiliations":[],"preferred":false,"id":363475,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wright, D.S.","contributorId":56799,"corporation":false,"usgs":true,"family":"Wright","given":"D.S.","email":"","affiliations":[],"preferred":false,"id":363477,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70010272,"text":"70010272 - 1979 - Initiation and development of the southern California uplift along its northern margin","interactions":[],"lastModifiedDate":"2025-09-05T16:14:37.25027","indexId":"70010272","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Initiation and development of the southern California uplift along its northern margin","docAbstract":"Analysis of three first-order leveling lines that traverse the White Wolf fault (site of the 1952 M = 7.7 earthquake), each resurveyed nine times between 1926 and 1974, reveals probable preseismic tilting, major coseismic movements, and a spatial association between these movements and the subsequently recognized southern California uplift. In examining the vertical control record, we have both searched for evidence of systematic errors and excluded from consideration portions of the lines contaminated by subsurface fluid and gas extraction. Movements have been referred to an invariant datum based on the 1926 position of tidal BM 8 in San Pedro, corrected for subsequent eustatic sea-level change.
An 8 μrad up-to-the-north preseismic tilt (6 cm/7.5 km) was apparently recorded on two adjacent line segments within 10 km of the 1952 epicenter between 1942 and 1947. It is possible, however, that this tilt was in part caused by extraction-induced subsidence at one of the six releveled benchmarks. Data also show evidence of episodic tilts that are not earthquake related. At the junction of the Garlock and San Andreas faults, for example, an ≥5 μrad up-to-the-north tilt (7.2 cm/≤16 km) took place between Lebec and Grapevine within three months during 1964.
Comparison of the 1947 and 1953 surveys, which includes the coseismic interval, shows that the SW-fault end (nearest the epicenter) and the central fault reach sustained four times the uplift recorded at the NE end of the fault (+72 cm SW, +53 cm Central, +16 cm NE). A regional postseismic uplift of 4 cm extended ≥25 km to either side of the fault after the main event, from 1953 to 1956. An interval of relative quiescence followed at least through 1959, in which the elevation change did not exceed ±3 cm.
The detailed pattern of aseismic uplift demonstrates that movement proceeded in space—time pulses: one half of the uplift at the SW-fault end and extending southward occurred between 1959 and 1961, one half of the uplift at the NE-fault end and extending eastward occurred between 1961 and 1965, while the central fault reach sustained successive pulses of subsidence, uplift, and collapse (−4 cm, 1953–1960; +7 cm, 1960–1965; −2 cm, 1965–1970). In addition, the number of aftershocks concentrated near the fault ends increased in the NE relative to the SW from 1952 to 1974. These observations suggest that the aseismic uplift may have migrated northeastward from 1959 to 1965 at an approximate rate of 7–16 km/yr.
Evidence for a mechanical coupling between the earthquake and the subsequent aseismic uplift is equivocal. At both fault ends, the major NWbounding flexure or tilted front of the southern California uplift is spatially coincident with the coseismic flexure that preceded it. In addition, the postulated migration of vertical deformation is similar to the 1952 seismic event in which the rupture initiated at the SW end of the fault and then propagated to the NE-fault end. However, the spatial distribution of aseismic uplift, nearly identical at both fault ends and to the south and east, and near zero in the central fault reach, is distinctly different from the nonuniform and localized coseismic deformation.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90234-8","issn":"00401951","usgsCitation":"Stein, R., Thatcher, W., and Castle, R.O., 1979, Initiation and development of the southern California uplift along its northern margin: Tectonophysics, v. 52, no. 1-4, p. 301-302, https://doi.org/10.1016/0040-1951(79)90234-8.","productDescription":"2 p.","startPage":"301","endPage":"302","costCenters":[],"links":[{"id":218858,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"southern California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -120.7291858900493,\n 35.46353030675584\n ],\n [\n -120.7291858900493,\n 32.603965801918534\n ],\n [\n -114.22074772045107,\n 32.603965801918534\n ],\n [\n -114.22074772045107,\n 35.46353030675584\n ],\n [\n -120.7291858900493,\n 35.46353030675584\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a3befe4b0c8380cd62948","contributors":{"authors":[{"text":"Stein, R.S.","contributorId":8875,"corporation":false,"usgs":true,"family":"Stein","given":"R.S.","email":"","affiliations":[],"preferred":false,"id":358493,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Thatcher, W.","contributorId":32669,"corporation":false,"usgs":true,"family":"Thatcher","given":"W.","email":"","affiliations":[],"preferred":false,"id":358494,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Castle, R. O.","contributorId":79880,"corporation":false,"usgs":true,"family":"Castle","given":"R.","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":358495,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70010377,"text":"70010377 - 1979 - Strain pattern represented by scarps formed during the earthquakes of October 2, 1915, Pleasant Valley, Nevada","interactions":[],"lastModifiedDate":"2025-09-04T15:43:41.678144","indexId":"70010377","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Strain pattern represented by scarps formed during the earthquakes of October 2, 1915, Pleasant Valley, Nevada","docAbstract":"The pattern of scarps developed during the earthquakes of October 2, 1915, in Pleasant Valley, Nevada, may have formed as a result of a modern stress system acting on a set of fractures produced by an earlier stress system which was oriented differently. Four major scarps developed in a right-stepping, en-echelon pattern suggestive of left-lateral slip across the zone and an extension axis oriented approximately S85°W. The trend of the zone is N25°E. However, the orientation of simple dip-slip on most segments trending approximately N20—40° E and a right-lateral component of displacement on several N- and NW-trending segments of the scarps indicate that the axis of regional extension was oriented between N50° and 70° W, normal to the zone.
The cumulative length of the scarps is 60 km, average vertical displacement 2 m, and the maximum vertical displacement near the Pearce School site 5.8 m. Almost everywhere the 1915 scarps formed along an older scarp line, and in some places older scarps represent multiple previous events. The most recent displacement event prior to 1915 is interpreted to have occurred more than 6600 years ago, but possibly less than 20,000 years ago. Some faults expressed by older scarps that trend northwest were not reactivated in 1915, possibly because they are oriented at a low angle with respect to the axis of modern regional extension.
The 1915 event occurred in an area of overlap of three regional fault trends oriented northwest, north, and northeast and referred to, respectively, as the Oregon—Nevada, Northwest Nevada, and Midas—Battle Moutain trends. Each of these trends may have developed at a different time; the Oregon—Nevada trend was possibly the earliest and developed in Late Miocene time (Stewart et al. 1975). Segments of the 1915 scarps ar
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90274-9","issn":"00401951","usgsCitation":"Wallace, R.E., 1979, Strain pattern represented by scarps formed during the earthquakes of October 2, 1915, Pleasant Valley, Nevada: Tectonophysics, v. 52, no. 1-4, p. 599-599, https://doi.org/10.1016/0040-1951(79)90274-9.","productDescription":"1 p.","startPage":"599","endPage":"599","costCenters":[],"links":[{"id":218719,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Pleasant Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -115.57276643805419,\n 40.752189211754455\n ],\n [\n -115.57276643805419,\n 40.68420641169672\n ],\n [\n -115.4573307107092,\n 40.68420641169672\n ],\n [\n -115.4573307107092,\n 40.752189211754455\n ],\n [\n -115.57276643805419,\n 40.752189211754455\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b9899e4b08c986b31c0c0","contributors":{"authors":[{"text":"Wallace, R. E.","contributorId":6823,"corporation":false,"usgs":true,"family":"Wallace","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":358777,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010376,"text":"70010376 - 1979 - Earthquakes and fault creep on the northern San Andreas fault","interactions":[],"lastModifiedDate":"2025-09-03T16:43:52.933574","indexId":"70010376","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Earthquakes and fault creep on the northern San Andreas fault","docAbstract":"At present there is an absence of both fault creep and small earthquakes on the northern San Andreas fault, which had a magnitude 8 earthquake with 5 m of slip in 1906. The fault has apparently been dormant after the 1906 earthquake. One possibility is that the fault is ‘locked’ in some way and only produces great earthquakes. An alternative possibility, presented here, is that the lack of current activity on the northern San Andreas fault is because of a lack of sufficient elastic strain after the 1906 earthquake. This is indicated by geodetic measurements at Fort Ross in 1874, 1906 (post-earthquake), and 1969, which show that the strain accumulation in 1969 (69 · 10−6 engineering strain) was only about one-third of the strain release (rebound) in the 1906 earthquake (200 · 10−6 engineering strain).
The large difference in seismicity before and after 1906, with many strong local earthquakes from 1836 to 1906, but only a few strong earthquakes from 1906 to 1976, also indicates a difference of elastic strain.
The geologic characteristics (serpentine, fault straightness) of most of the northern San Andreas fault are very similar to the characteristics of the fault south of Hollister, where fault creep is occurring. Thus, the current absence of fault creep on the northern fault segment is probably due to a lack of sufficient elastic strain at the present time.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90278-6","issn":"00401951","usgsCitation":"Nason, R., 1979, Earthquakes and fault creep on the northern San Andreas fault: Tectonophysics, v. 52, no. 1-4, p. 604-604, https://doi.org/10.1016/0040-1951(79)90278-6.","productDescription":"1 p.","startPage":"604","endPage":"604","costCenters":[],"links":[{"id":218645,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"northern San Andreas fault","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -123.1499918292879,\n 41.06933328404864\n ],\n [\n -121.84407885980457,\n 38.105716092362385\n ],\n [\n -119.29367963965812,\n 34.41809055699687\n ],\n [\n -118.21710522193753,\n 34.83484578736363\n ],\n [\n -122.06386648472477,\n 40.96790016170016\n ],\n [\n -123.1499918292879,\n 41.06933328404864\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a050fe4b0c8380cd50c45","contributors":{"authors":[{"text":"Nason, R.","contributorId":94032,"corporation":false,"usgs":true,"family":"Nason","given":"R.","affiliations":[],"preferred":false,"id":358776,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012443,"text":"70012443 - 1979 - On radon emanation as a possible indicator of crustal deformation","interactions":[],"lastModifiedDate":"2025-09-05T16:34:33.043296","indexId":"70012443","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"On radon emanation as a possible indicator of crustal deformation","docAbstract":"Radon emanation has been monitored in shallow capped holes by a Tracketch method along several active faults and in the vicinity of some volcanoes and underground nuclear explosions. The measured emanation shows large temporal variations that appear to be partly related to crustal strain changes. This paper proposes a model that may explain the observed tectonic variations in radon emanation, and explores the possibility of using radon emanation as an indicator of crustal deformation. In this model the emanation variation is assumed to be due to the perturbation of near-surface profile of radon concentration in the soil gas caused by a change in the vertical flow rate of the soil gas which, in turn, is caused by the crustal deformation. It is shown that, for a typical soil, a small change in the flow rate (3 · 10−4 cm sec−1) can effect a significant change (a factor of 2) in radon emanation detected at a fixed shallow depth (0.7 m). The radon concentration profile has been monitored at several depths at a selected site to test the model. The results appear to be in satisfactory agreement.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90215-4","issn":"00401951","usgsCitation":"King, C., 1979, On radon emanation as a possible indicator of crustal deformation: Tectonophysics, v. 52, no. 1-4, p. 120-120, https://doi.org/10.1016/0040-1951(79)90215-4.","productDescription":"1 p.","startPage":"120","endPage":"120","costCenters":[],"links":[{"id":222353,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a6da6e4b0c8380cd75252","contributors":{"authors":[{"text":"King, Chi-Yu","contributorId":74140,"corporation":false,"usgs":true,"family":"King","given":"Chi-Yu","affiliations":[],"preferred":false,"id":363593,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012482,"text":"70012482 - 1979 - Early 20th-century uplift of the northern Peninsular Ranges province of southern California","interactions":[],"lastModifiedDate":"2025-09-05T16:19:29.965797","indexId":"70012482","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Early 20th-century uplift of the northern Peninsular Ranges province of southern California","docAbstract":"Repeated leveling in the northern Peninsular Ranges province identifies an early 20thcentury episode of crustal upwarping in southern California. The episodic vertical movement is broadly bracketed between 1897 and 1934, and the main deformation is bracketed within 1906–1914 and involved regional up-to-the-northeast tilting of the Santa Ana block of as much as 4 · 10−6 rad and elevation changes exceeding 0.4 m in the Perris block and parts of the San Jacinto block, Transverse Ranges, and the Mohave block. Primary tide station records containing occasional entries since 1853 at San Pedro and San Diego show no evidence of episodic crustal movement, suggesting that the uplifted area hinged along coastal fault zones forming the west boundary of the Santa Ana block.
Physiographic features and recent studies of Quaternary marine terraces by others show that this episode of regional tilting and uplift is a part of the continuing tectonic process in southern California. A crude, questionable coincidence exists between the uplift episode and a period of increased seismicity (1890–1923) in the northern Peninsular Ranges characterized by a number of moderate-size (M > 6) earthquakes on NW-trending strike-slip faults. However, releveling data are too sparse to associate the uplift development clearly with any one event.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90230-0","issn":"00401951","usgsCitation":"Wood, S.H., and Elliott, M.R., 1979, Early 20th-century uplift of the northern Peninsular Ranges province of southern California: Tectonophysics, v. 52, no. 1-4, p. 249-265, https://doi.org/10.1016/0040-1951(79)90230-0.","productDescription":"17 p.","startPage":"249","endPage":"265","costCenters":[],"links":[{"id":222082,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"southern California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -120.7291858900493,\n 35.46353030675584\n ],\n [\n -120.7291858900493,\n 32.603965801918534\n ],\n [\n -114.22074772045107,\n 32.603965801918534\n ],\n [\n -114.22074772045107,\n 35.46353030675584\n ],\n [\n -120.7291858900493,\n 35.46353030675584\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0473e4b0c8380cd509c1","contributors":{"authors":[{"text":"Wood, Spencer H. 0000-0002-5794-2619","orcid":"https://orcid.org/0000-0002-5794-2619","contributorId":16111,"corporation":false,"usgs":false,"family":"Wood","given":"Spencer","email":"","middleInitial":"H.","affiliations":[{"id":6934,"text":"University of Washington","active":true,"usgs":false}],"preferred":false,"id":363723,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Elliott, Michael R.","contributorId":291274,"corporation":false,"usgs":false,"family":"Elliott","given":"Michael","middleInitial":"R.","affiliations":[{"id":62651,"text":"Department of Biological & Marine Sciences, University of Hull and International Estuarine & Coastal Specialists (IECS)","active":true,"usgs":false}],"preferred":false,"id":363722,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70012207,"text":"70012207 - 1979 - Late Cenozoic uplift of the southwestern Colorado Plateau and adjacent lower Colorado River region","interactions":[],"lastModifiedDate":"2025-09-02T16:43:13.240404","indexId":"70012207","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Late Cenozoic uplift of the southwestern Colorado Plateau and adjacent lower Colorado River region","docAbstract":"Rocks deposited near sea level under marine, estuarine, and lacustrine conditions, and located along the course of the lower Colorado River from the mouth of the Grand Canyon as far as the Mexican border, have been displaced to present positions as high as 880 m a.s.l. and as low as 1600 m b.s.l. The rocks include the marine and estuarine Bouse Formation and the lacustrine or marine Hualapai Limestone Member of the Muddy Creek Formation. A profile joining spot elevations that represent the highest erosional remnants of these rocks preserved at any one locality gives an approximation (in most cases a minimum value) for the uplift or downdropping of the region relative to sea level since about 5.5 m.y. ago, the K/Ar age of the most widespread and critical unit. The profile shows that most of the lower Colorado region has risen at least 550 m through broad and rather uniform upwarping and at an average rate of about 100 m/m.y. In addition to these 550 m, the nearby Colorado Plateau has risen by discrete movement along Wheeler fault, which is parallel to and about 8 km west of the plateau's edge, to a total uplift of at least 880 m, at a rate that may be as high as 160 m/m.y. Before warping and faulting, the top of the plateau was about 1100 m above the fill of adjacent basins; the top of this fill probably was at or a little below sea level. The profile shows two major south-facing rises in slope. The bigger one, near Yuma, occurs where the profile intersects the northwest-trending San Andreas-Salton trough system of faults; it is interpreted as rifting resulting from transcurrent movement along the faults. At the Mexican border, the base of the Bouse Formation is 1600 m b.s.l., which corresponds to a rate of subsidence since the beginning of Bouse time that may be as high as 290 m/.m.y. The top of the Bouse is at 1000 m b.s.l., corresponding to a rate of subsidence of about 180 m/m.y. In this area, the “older marine sedimentary rocks” of Olmsted et al., (1973) occur as much as 2100 m b.s.l. These rocks are evidence for marine invasion and deformation that predate the Bouse Formation. The second rise in slope occurs at the intersection with a regional northwest-trending lineament that separates widely different geologic terranes and is associated with extensive Miocene volcanism. This lineament may represent an old transform fault similar in geologic function to the present San Andreas system.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90292-0","issn":"00401951","usgsCitation":"Lucchitta, I., 1979, Late Cenozoic uplift of the southwestern Colorado Plateau and adjacent lower Colorado River region: Tectonophysics, v. 61, no. 1-3, p. 63-95, https://doi.org/10.1016/0040-1951(79)90292-0.","productDescription":"33 p.","startPage":"63","endPage":"95","costCenters":[],"links":[{"id":222340,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona, California, Colorado, Nevada","otherGeospatial":"Colorado Plateau","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -114.9408782399043,\n 38.844788908296735\n ],\n [\n -114.9408782399043,\n 32.199963398730716\n ],\n [\n -108.69541610940806,\n 32.36496801287734\n ],\n [\n -108.85250768215414,\n 36.85087011455222\n ],\n [\n -103.6331527855288,\n 37.334529578686464\n ],\n [\n -103.9722485436863,\n 40.78887688227549\n ],\n [\n -108.87501297416733,\n 40.92333340337099\n ],\n [\n -109.12890852443115,\n 37.103318707956426\n ],\n [\n -114.44844110582223,\n 38.313677510457254\n ],\n [\n -114.9408782399043,\n 38.844788908296735\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"61","issue":"1-3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4546e4b0c8380cd6719a","contributors":{"authors":[{"text":"Lucchitta, Ivo","contributorId":94291,"corporation":false,"usgs":true,"family":"Lucchitta","given":"Ivo","email":"","affiliations":[],"preferred":false,"id":362992,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012442,"text":"70012442 - 1979 - Monitoring massive fracture growth at 2-km depths using surface tiltmeter arrays","interactions":[],"lastModifiedDate":"2025-09-03T16:33:51.216118","indexId":"70012442","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Monitoring massive fracture growth at 2-km depths using surface tiltmeter arrays","docAbstract":"Tilt due to massive hydraulic fractures induced in sedimentary rocks at depths of up to 2.2 km have been recorded by surface tiltmeters. Injection of fluid volumes up to 4 · 105 liters and masses of propping agent up to 5 · 105 kg is designed to produce fractures approximately 1 km long, 50–100 m high and about 1 cm wide. The surface tilt data adequately fit a dislocation model of a tensional fault in a half-space. Theoretical and observational results indicate that maximum tilt occurs at a distance off the strike of the fracture equivalent to 0.4 of the depth to the fracture. Azimuth and extent of the fracture deduced from the geometry of the tilt field agree with other kinds of geophysical measurements. Detailed correlation of the tilt signatures with pumping parameters (pressure, rate, volume, mass) have provided details on asymmetry in geometry and growth rate. Whereas amplitude variations in tilt vary inversely with the square of the depth, changes in flow rate or pressure gradient can produce a cubic change in width. These studies offer a large-scale experimental approach to the study of problems involving fracturing, mass transport, and dilatancy processes.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90283-X","issn":"00401951","usgsCitation":"Wood, M., 1979, Monitoring massive fracture growth at 2-km depths using surface tiltmeter arrays: Tectonophysics, v. 52, no. 1-4, p. 643-643, https://doi.org/10.1016/0040-1951(79)90283-X.","productDescription":"1 p.","startPage":"643","endPage":"643","costCenters":[],"links":[{"id":222352,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5dbee4b0c8380cd70582","contributors":{"authors":[{"text":"Wood, M.D.","contributorId":63930,"corporation":false,"usgs":true,"family":"Wood","given":"M.D.","email":"","affiliations":[],"preferred":false,"id":363592,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012502,"text":"70012502 - 1979 - Aging and strain softening model for episodic faulting","interactions":[],"lastModifiedDate":"2025-09-03T16:37:38.306427","indexId":"70012502","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Aging and strain softening model for episodic faulting","docAbstract":"Episodic slip on shallow crustal faults can be qualitatively explained by postulating a fault constitutive law that is the superposition of two limiting material responses: (1) strain softening after peak stress during large strain rates, and (2) strength (peak stress) recovery during aging at small strain rates. A single law permits a variety of seismic and aseismic phenomena to occur over a range of space and time scales. Specific cases are determined by the spatial variation of material constants, recent deformation history, crustal rigidity, and remote forcing.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90280-4","issn":"00401951","usgsCitation":"Stuart, W.D., 1979, Aging and strain softening model for episodic faulting: Tectonophysics, v. 52, no. 1-4, p. 613-626, https://doi.org/10.1016/0040-1951(79)90280-4.","productDescription":"14 p.","startPage":"613","endPage":"626","costCenters":[],"links":[{"id":222358,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e90ce4b0c8380cd4806f","contributors":{"authors":[{"text":"Stuart, William D. stuart@usgs.gov","contributorId":3223,"corporation":false,"usgs":true,"family":"Stuart","given":"William","email":"stuart@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":363767,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012481,"text":"70012481 - 1979 - Marine terrace deformation, San Diego County, California","interactions":[],"lastModifiedDate":"2025-09-04T16:26:32.097596","indexId":"70012481","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Marine terrace deformation, San Diego County, California","docAbstract":"The NW—SE trending southern California coastline between the Palos Verdes Peninsula and San Diego roughly parallels the southern part and off-shore extension of the dominantly right-lateral, strike-slip, Newport—Inglewood fault zone. Emergent marine terraces between Newport Bay and San Diego record general uplift and gentle warping on the northeast side of the fault zone throughout Pleistocene time. Marine terraces on Soledad Mt. and Point Loma record local differential uplift (maximum 0.17 m/ka) during middle to late Pleistocene time on the southwest side of the fault (Rose Canyon fault) near San Diego.
The broad Linda Vista Mesa (elev. 70–120 m) in the central part of coastal San Diego County, previously thought to be a single, relatively undeformed marine terrace of Plio—Pleistocene age, is a series of marine terraces and associated beach ridges most likely formed during sea-level highstands throughout Pleistocene time. The elevations of the terraces in this sequence gradually increase northwestward to the vicinity of San Onofre, indicating minor differential uplift along the central and northern San Diego coast during Pleistocene time. The highest, oldest terraces in the sequence are obliterated by erosional dissection to the northwest where uplift is greatest.
Broad, closely spaced (vertically) terraces with extensive beach ridges were the dominant Pleistocene coastal landforms in central San Diego County where the coastal slope is less than 1% and uplift is lowest. The beach ridges die out to the northwest as the broad low terraces grade laterally into narrower, higher, and more widely spaced (vertically) terraces on the high bluffs above San Onofre where the coastal slope is 20–30% and uplift is greatest. At San Onofre the terraces slope progressively more steeply toward the ocean with increasing elevation, indicating continuous southwest tilt accompanying uplift from middle to late Pleistocene time. This southwest tilt is also recorded in the asymmetrical valleys of major local streams where strath terraces occur only on the northeast side of NW—SE-trending valley segments.
The deformational pattern (progressively greater uplift to the northwest with slight southwest tilt) recorded in the marine and strath terraces of central and northern coastal San Diego County conforms well with the historic pattern derived by others from geodetic data. It is not known how much of the Santa Ana structural block (between the Newport—Inglewood and the Elsinore fault zones) is affected by this deformational pattern.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90254-3","issn":"00401951","usgsCitation":"McCrory, P., and Lajoie, K.R., 1979, Marine terrace deformation, San Diego County, California: Tectonophysics, v. 52, no. 1-4, p. 407-408, https://doi.org/10.1016/0040-1951(79)90254-3.","productDescription":"2 p.","startPage":"407","endPage":"408","costCenters":[],"links":[{"id":222081,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","county":"San Diego County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"id\":221,\"properties\":{\"name\":\"San 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P.A.","contributorId":96287,"corporation":false,"usgs":true,"family":"McCrory","given":"P.A.","email":"","affiliations":[],"preferred":false,"id":363721,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lajoie, K. R.","contributorId":6828,"corporation":false,"usgs":true,"family":"Lajoie","given":"K.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":363720,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70012485,"text":"70012485 - 1979 - Deep structure under Yellowstone National Park U.S.A.: A continental \"hot spot\"","interactions":[],"lastModifiedDate":"2025-09-03T16:20:18.223033","indexId":"70012485","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Deep structure under Yellowstone National Park U.S.A.: A continental \"hot spot\"","docAbstract":"In order to understand the origin of long-lived loci of volcanism (sometimes called “hot spots”) and their possible role in global tectonic processes, it is essential to know their deep structure. Even though some work has been done on the crustal, upper-mantle, and deep-mantle structure under some of these “hot spots”, the picture is far from clear. In an attempt to study the structure under the Yellowstone National Park U.S.A., which is considered to be such a “hot spot”, we recorded teleseisms using 26 telemetered seismic stations and three groups of portable stations. The network was operated within a 150 km radius centered on the Yellowstone caldera, the major, Quaternary volcanic feature of the Yellowstone region. Teleseismic delays of about 1.5 sec are found inside the caldera, and the delays remain high over a 100 km wide area around the caldera. The spatial distribution and magnitude of the delays indicate the presence of a large body of low-velocity material with horizontal dimensions corresponding approximately to the caldera size (40 km × 80 km) near the surface and extending to a depth of 200–250 km under the caldera. Using ray-tracing and inversion techniques, it is estimated that the compressional velocity inside the anomalous body is lower than in the surrounding rock by about 15% in the upper crust and by 5% in the lower crust and upper mantle. It is postulated that the body is partly composed of molten rock with a high degree of partial melting at shallow depths and is responsible for the observed Yellowstone volcanism. The large size of the partially molten body, taken together with its location at the head of a 350 km zone of volcanic propagation along the axis of the Snake River Plain, indicates that the volcanism associated with Yellowstone has its origin below the lithosphere and is relatively stationary with respect to plate motion. Using our techniques, we are unable to detect any measurable velocity contrast in the mantle beneath the low-velocity body, and, hence, we are unable to determine whether the Yellowstone melting anomaly is associated with a deep heat source or with any deep phenomenon such as a convection plume, chemical plume, or gravitational anchor.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90030-1","issn":"00401951","usgsCitation":"Iyer, H.M., 1979, Deep structure under Yellowstone National Park U.S.A.: A continental \"hot spot\": Tectonophysics, v. 56, no. 1-2, p. 165-197, https://doi.org/10.1016/0040-1951(79)90030-1.","productDescription":"33 p.","startPage":"165","endPage":"197","costCenters":[],"links":[{"id":222144,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"Yellowstone National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -111.03532659212517,\n 45.01881690702004\n ],\n [\n -111.03532659212517,\n 43.79708737827522\n ],\n [\n -109.5802983585797,\n 43.79708737827522\n ],\n [\n -109.5802983585797,\n 45.01881690702004\n ],\n [\n -111.03532659212517,\n 45.01881690702004\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"56","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059fe2be4b0c8380cd4eb70","contributors":{"authors":[{"text":"Iyer, H. M.","contributorId":17997,"corporation":false,"usgs":true,"family":"Iyer","given":"H.","middleInitial":"M.","affiliations":[],"preferred":false,"id":363728,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010440,"text":"70010440 - 1979 - Changes in rate of fault creep","interactions":[],"lastModifiedDate":"2025-09-04T16:06:32.354124","indexId":"70010440","displayToPublicDate":"2003-04-09T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Changes in rate of fault creep","docAbstract":"Aseismic slip or fault creep is occurring on many faults in California. Although the creep rates are generally less than 10 mm/yr in most regions, the maximum observed rate along the San Andreas fault between San Juan Bautista and Gold Hill in central California exceeds 30 mm/yr. Changes in slip rates along a 162 km segment of the San Andreas fault in this region have occurred at approximately the same time at up to nine alinement array sites. Rates of creep on the fault near the epicenters of moderate earthquakes (ML 4–6) vary for periods of several years, decreasing before the main shocks and increasing thereafter, in agreement with prior observations based on creepmeter results. The change of surface slip rate is most pronounced within the epicentral region defined by aftershocks, but records from sites at distances up to 100 km show similar variations. Additionally, some variations in rate, also apparently consistent among many sites, have a less obvious relation with seismic activity and have usually taken place over shorter periods. Not all sites exhibit a significant variation in rate at the time of a regional change, and the amplitudes of the change at nearby sites are not consistently related. The time intervals between measurements at the nine array sites during a given period have not always been short with respect to the intervals between surveys at one site; hence, uneven sampling intervals may bias the results slightly. Anomalies in creep rates thus far observed, therefore, have not been demonstrably consistent precursors to moderate earthquakes; and in the cases when an earthquake has followed a long period change of rate, the anomaly has not specified time, place, or magnitude with a high degree of certainty. The consistency of rate changes may represent a large scale phenomenon that occurs along much of the San Andreas transform plate boundary.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90266-X","issn":"00401951","usgsCitation":"Harsh, P., 1979, Changes in rate of fault creep: Tectonophysics, v. 52, no. 1-4, p. 519-519, https://doi.org/10.1016/0040-1951(79)90266-X.","productDescription":"1 p.","startPage":"519","endPage":"519","costCenters":[],"links":[{"id":218647,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"San Andreas fault","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -123.49111683709873,\n 41.23845484514334\n ],\n [\n -121.22954609997186,\n 37.147723728935766\n ],\n [\n -117.44018054284913,\n 33.754578338292035\n ],\n [\n -116.1951646206461,\n 33.81034080556368\n ],\n [\n -119.83129934259983,\n 37.519569891913555\n ],\n [\n -122.23061585176441,\n 41.35680615153203\n ],\n [\n -123.49111683709873,\n 41.23845484514334\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"52","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f421e4b0c8380cd4bb6f","contributors":{"authors":[{"text":"Harsh, P.","contributorId":59175,"corporation":false,"usgs":true,"family":"Harsh","given":"P.","email":"","affiliations":[],"preferred":false,"id":358934,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012416,"text":"70012416 - 1979 - Geology and tectonic development of the continental margin north of Alaska","interactions":[],"lastModifiedDate":"2025-09-02T16:51:24.052749","indexId":"70012416","displayToPublicDate":"2003-04-08T00:00:00","publicationYear":"1979","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Geology and tectonic development of the continental margin north of Alaska","docAbstract":"The continental margin north of Alaska, as interpreted from seismic reflection profiles, is of the Atlantic type and consists of three sectors of contrasting structure and stratigraphy. The Chukchi sector, on the west, is characterized by the deep late Mesozoic and Tertiary North Chukchi basin and the Chukchi Continental Borderland. The Barrow sector of central northern Alaska is characterized by the Barrow arch and a moderately thick continental terrace build of Albian to Tertiary clastic sediment. The terrace sedimentary prism is underlain by lower Paleozoic metasedimentary rocks. The Barter Island sector of northeastern Alaska and Yukon Territory is inferred to contain a very thick prism of Jurassic, Cretaceous and Tertiary marine and nonmarine clastic sediment. Its structure is dominated by a local deep Tertiary depocenter and two regional structural arches.
We postulate that the distinguishing characteristics of the three sectors are inherited from the configuration of the rift that separated arctic Alaska from the Canadian Arctic Archipelago relative to old pre-rift highlands, which were clastic sediment sources. Where the rift lay relatively close to northern Alaska, in the Chukchi and Barter Island sectors, and locally separated Alaska from the old source terranes, thick late Mesozoic and Tertiary sedimentary prisms extend farther south beneath the continental shelf than in the intervening Barrow sector. The boundary between the Chukchi and Barrow sectors is relatively well defined by geophysical data, but the boundary between the Barrow and Barter Island sectors can only be inferred from the distribution and thickness of Jurassic and Cretaceous sedimentary rocks. These boundaries may be extensions of oceanic fracture zones related to the rifting that is postulated to have opened the Canada Basin, probably beginning during the Early Jurassic.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(79)90050-7","issn":"00401951","usgsCitation":"Grantz, A., Eittreim, S., and Dinter, D.A., 1979, Geology and tectonic development of the continental margin north of Alaska: Tectonophysics, v. 59, no. 1-4, p. 263-291, https://doi.org/10.1016/0040-1951(79)90050-7.","productDescription":"29 p.","startPage":"263","endPage":"291","costCenters":[],"links":[{"id":221893,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -172.11589499397513,\n 73.56845265796551\n ],\n [\n -172.11589499397513,\n 66.39262903165613\n ],\n [\n -140.49034024384332,\n 66.39262903165613\n ],\n [\n -140.49034024384332,\n 73.56845265796551\n ],\n [\n -172.11589499397513,\n 73.56845265796551\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"59","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a243fe4b0c8380cd57f06","contributors":{"authors":[{"text":"Grantz, Arthur agrantz@usgs.gov","contributorId":2585,"corporation":false,"usgs":true,"family":"Grantz","given":"Arthur","email":"agrantz@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":363487,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Eittreim, Stephen","contributorId":102553,"corporation":false,"usgs":true,"family":"Eittreim","given":"Stephen","email":"","affiliations":[],"preferred":false,"id":363488,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dinter, David A.","contributorId":104010,"corporation":false,"usgs":true,"family":"Dinter","given":"David","middleInitial":"A.","affiliations":[],"preferred":false,"id":363489,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}