Seismotectonics
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Seismicity, Seismotectonics and Preliminary Earthquake Hazard Analysis of the Teton Region, WY
FINAL TECHNICAL REPORT DEVELOPMENT OF EARTHQUAKE GROUND SHAKING HAZARD MAPS FOR THE YELLOWSTONE- JACKSON HOLE-STAR VALLEY, WYOMING Submitted to the U.S. Geological Survey Under the National Earthquake Hazards Reduction Program Program Element II Evaluate Urban Hazard and Risk USGS Award 05HQGR0026 Prepared by Bonnie Jean Pickering White Department of Geology and Geophysics The University of Utah Salt Lake City, UT 94112 and Robert B. Smith Department of Geology and Geophysics The University of Utah Salt Lake City, UT 94112 Principal Investigator Ivan Wong Seismic Hazards Group URS Corporation 1333 Broadway, Suite 800, Oakland, CA 94612 Phone: (510) 874-3014, Fax: (510) 874-3268 E-mail: [email protected] 26 September 2006 __________________________ This research was supported by the U. S. Geological Survey (USGS), Department of the Interior, under USGS Award Number 05HQGR0026. The views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily representing the official policies, either expressed or implied of the U.S. Government. PREFACE The Yellowstone-Jackson Hole-Star Valley corridor is located within the seismically and tectonically active Intermountain Seismic Belt in westernmost Wyoming and eastern Idaho. The corridor has the highest seismic hazard in the Intermountain U.S. based on the U.S. Geological Survey’s National Hazard Maps. The region contains the heavily visited Yellowstone and Teton National Parks and the rapidly growing areas of Jackson Hole and Star Valley. Although there has only been one large earthquake in this region in historical times (1959 moment magnitude [M] 7.5 Hebgen Lake), abundant geologic evidence exists for the past occurrence of surface-faulting earthquakes of M 7 or greater. -
Chapter 2 the Evolution of Seismic Monitoring Systems at the Hawaiian Volcano Observatory
Characteristics of Hawaiian Volcanoes Editors: Michael P. Poland, Taeko Jane Takahashi, and Claire M. Landowski U.S. Geological Survey Professional Paper 1801, 2014 Chapter 2 The Evolution of Seismic Monitoring Systems at the Hawaiian Volcano Observatory By Paul G. Okubo1, Jennifer S. Nakata1, and Robert Y. Koyanagi1 Abstract the Island of Hawai‘i. Over the past century, thousands of sci- entific reports and articles have been published in connection In the century since the Hawaiian Volcano Observatory with Hawaiian volcanism, and an extensive bibliography has (HVO) put its first seismographs into operation at the edge of accumulated, including numerous discussions of the history of Kīlauea Volcano’s summit caldera, seismic monitoring at HVO HVO and its seismic monitoring operations, as well as research (now administered by the U.S. Geological Survey [USGS]) has results. From among these references, we point to Klein and evolved considerably. The HVO seismic network extends across Koyanagi (1980), Apple (1987), Eaton (1996), and Klein and the entire Island of Hawai‘i and is complemented by stations Wright (2000) for details of the early growth of HVO’s seismic installed and operated by monitoring partners in both the USGS network. In particular, the work of Klein and Wright stands and the National Oceanic and Atmospheric Administration. The out because their compilation uses newspaper accounts and seismic data stream that is available to HVO for its monitoring other reports of the effects of historical earthquakes to extend of volcanic and seismic activity in Hawai‘i, therefore, is built Hawai‘i’s detailed seismic history to nearly a century before from hundreds of data channels from a diverse collection of instrumental monitoring began at HVO. -
Seismotectonics of the April 25, 1992, Petrolia Earthquake and The
TECTONICS, VOL. 14, NO. 5, PAGES, 1095-1103,OCTOBER 1995 Seismotectonicsof the April 25, 1992, Petrolla earthquake and the Mendocino triple junction region Yuichiro Tanioka, Kenji Satake,and Larry Ruff Departmentof GeologicalSciences, University of Michigan, Ann Arbor Abstract. The April 25, 1992, Petrolia earthquake(Ms 7.1) 124ø34.47'W.The parametersof the secondaftershock (AF2) are occurredat the southerntip of the Cascadiasubduction zone. origin time 11:18:25.8 (GMT); location, 40ø23.40'N, This is thelargest thrust earthquake ever recorded instrumentally 124ø34.30'W.These earthquakes occurred near Cape Mendocino, in the Cascadiasubduction zone. The earthquakewas followed where the Pacific, North American, and Gorda plates meet by two large strike-slip aftershocks(both Ms 6.6). Moment (Figure 1). The Gorda plate is the southernpart of the Juan de releaseof eachof theearthquakes is as follows: 4.0 x 1019Nm in Fuca plate, south of the Blanco Fracture Zone. In order to the first 10 s for themainshock, 0.7 x 1019Nm in the first 8 s for explain the spaceproblem betweenthe Blanco FractureZone in the first aftershock,and 0.9 x 1019Nm in the first 2 s for the the north and the Mendocino Fault Zone in the south, Wilson second aftershock. These indicate that the mainshock and each of [1986] claimed that the Gorda plate is not a rigid plate and the aftershocksmay have different tectonicbackgrounds. The deforms internally. He called it the Gorda deformation zone bestdepth estimates of the mainshockand the two aftershocksare (GDZ). Seismicitystudies by Smithand Knapp [1980] andSmith 14 km, 18 km, and 24 km, respectively.The slip directionof the eta/. -
IV. Environmental Impact Analysis D. Geology and Soils
IV. Environmental Impact Analysis D. Geology and Soils 1. Introduction This section of the Draft EIR analyzes the proposed Project’s potential impacts with regard to geology and soils. The analysis includes an evaluation of the potential geologic hazards associated with fault rupture, seismic ground shaking, liquefaction, landslides, inundation, other geologic conditions, and underlying soils. The analysis is based on the Geotechnical Engineering Evaluation prepared by Geotechnologies Inc., which is provided in Appendix D of this Draft EIR. 2. Environmental Setting a. Existing Conditions (1) Regional Geologic Setting The Project site is located in the northern portion of the Peninsular Ranges Geomorphic Province. The Peninsular Ranges are characterized by northwest-trending blocks of mountain ridges and sediment-floored valleys. The dominant geologic structural features are northwest trending fault zones that fade out to the northwest or terminate at east-trending reverse faults that form the southern margin of the Transverse Ranges. The Los Angeles Basin (Basin) is located at the northern end of the Peninsular Ranges Geomorphic Province. The Basin is bounded to the east and southeast by the Santa Ana Mountains and San Joaquin Hills and to the northwest by the Santa Monica Mountains. Over 22 million years ago, the Basin was a deep marine basin formed by tectonic forces between the North American and Pacific plates. Since that time, over five miles of marine and non-marine sedimentary rock as well as intrusive and extrusive igneous rocks have filled the basin. During the last two million years, defined by the Pleistocene and Holocene epochs, the Basin and surrounding mountain ranges have been uplifted to form City of Los Angeles USC Development Plan SCH. -
Activity of the Offshore Newport–Inglewood Rose Canyon Fault Zone, Coastal Southern California, from Relocated Microseismicity by Lisa B
Bulletin of the Seismological Society of America, Vol. 94, No. 2, pp. 747–752, April 2004 Activity of the Offshore Newport–Inglewood Rose Canyon Fault Zone, Coastal Southern California, from Relocated Microseismicity by Lisa B. Grant and Peter M. Shearer Abstract An offshore zone of faulting approximately 10 km from the southern California coast connects the seismically active strike-slip Newport–Inglewood fault zone in the Los Angeles metropolitan region with the active Rose Canyon fault zone in the San Diego area. Relatively little seismicity has been recorded along the off- shore Newport–Inglewood Rose Canyon fault zone, although it has long been sus- pected of being seismogenic. Active low-angle thrust faults and Quaternary folds have been imaged by seismic reflection profiling along the offshore fault zone, raising the question of whether a through-going, active strike-slip fault zone exists. We applied a waveform cross-correlation algorithm to identify clusters of microseis- micity consisting of similar events. Analysis of two clusters along the offshore fault zone shows that they are associated with nearly vertical, north-northwest-striking faults, consistent with an offshore extension of the Newport–Inglewood and Rose Canyon strike-slip fault zones. P-wave polarities from a 1981 event cluster are con- sistent with a right-lateral strike-slip focal mechanism solution. Introduction The Newport–Inglewood fault zone (NIFZ) was first clusters of microearthquakes within the northern and central identified as a significant threat to southern California resi- ONI-RC fault zone to examine the fault structure, minimum dents in 1933 when it generated the M 6.3 Long Beach earth- depth of seismic activity, and source fault mechanism. -
Multinational Partnership for Research in Earthquake System Science
Offshore South-Central California for the Community Fault Model Report for SCEC Award #15098 Submitted March 28, 2015 Investigators: Christopher Sorlien I. Project Overview Offshore South-Central California for the Community Fault Model A. Abstract The SCEC Community Fault Model in offshore central California and western Santa Barbara Channel is based on 2D fault traces published in the 1980s. There are abundant multichannel seismic reflection (MCS) data, including 3D data, which image the 3D faults. Notably, the right- lateral Hosgri fault is imaged by 3D MCS data to be gently to moderately E-dipping between about 1 and 3 km depth. Much of the effort was focused on northwest Santa Barbara Channel, because of publications proposing M~8 earthquakes on the North Channel – Pitas Point (Ventura) –San Cayetano fault system, and a publication modeling huge sea floor uplifts and tsunamis. This fault system con- tinues 120 km west of Ventura, to west of Pt. Conception where it interacts with the southern termination of the Hosgri fault. The upper 4 km to 7 km of many strands of this fault system are imaged. There are only two geometric segment boundaries in the offshore faults; one located 10 km west of UCSB, and the other being near Gaviota. One lower strand of the system, the Pitas Point-Ventura fault, is continuous for 75 km. There is no evidence for sea floor rupture of the off- shore 60 km of this fault in the last half million years, including since formation of the Last Gla- cial Maximum unconformity. Instead, deep fault slip has been absorbed by a tilting anticline forelimb. -
Seismicity Patterns in Southern California Before and After the 1994
U.S. DEPARTMENT OF THE INTERIOR U.S. GEOLOGICAL SURVEY Seismicity Patterns in Southern California Before and After the 1994 Northridge Earthquake: A Preliminary Report by Paul A. Reasenberg Open-File Report 95-484 This report is preliminary and has not been reviewed for conformity with U.S. Geological Survey edi torial standards. Any use of trade, product or firm names is for descriptive purposes only and does not imply endorsement by the U.S. Government. 1995 Menlo Park, CA 94025 INTRODUCTION This report describes seismicity patterns in southern California before and after the January 17, 1994 Northridge (Mw = 6.7) earthquake. The report is preliminary in the sense that it was prepared as soon as the necessary data became available. The observations presented below of seismicity one year before and up to 3 months after the Northridge earthquake were compiled on April 18, 1994. The observations of the second quarter-year of post-seismic activity (April 17 to July 17) were compiled the week of July 18, 1994. The scope of the report is limited to the description of seismi city patterns, and excludes analysis of the regional geology, static and dynamic stresses and deformations associated with the Northridge (or previous) earthquakes, or other factors that may be relevant to a full understanding of the regional tectonics. For a summary of the Northridge earthquake see Scientists of the U.S. Geological Survey and the Southern California Earthquake Center (1994). Various meanings have been ascribed to the term "pattern". Taken out of context, any "snapshot" or finite sample taken from nature will contain patterns. -
SCF2 NEHRP 02HQGR0041 Report.Final
Final Report Paleoseismology and Seismic Hazards of the San Cayetano Fault Zone 02HQGR0041 James F. Dolan Department of Earth Sciences University of Southern California Los Angeles, CA 90089-0740 (213) 740-8599 [email protected] Southern California (SC) Key Words: Neotectonics, Trench Investigations, Paleoseismology, Recurrence Interval Introduction and Rationale for Research: The San Cayetano Fault The San Cayetano fault is a major, north-dipping reverse fault that extends for 40 km along the northern edge of the Ventura Basin and westward into the Sespe Mountains (Figure 1). The fault has been mapped in detail both at the surface and in the subsurface by a number of researchers, including Schlueter (1976), Yeats (1983), Çemen (1977; 1989), Dibblee (1987, 1990a, 1990b, 1991), Rockwell (1988), Yeats et al. (1994), and Huftile and Yeats (1995a; 1995b; 1996). These studies reveal that the San Cayetano fault is separated into two major sections (or 'lobes') by the 4-km-wide, Sespe Creek lateral ramp near the city of Fillmore (Figure 2). The eastern, or ‘Modelo’ lobe (so named because of prominent exposures of the Miocene Modelo Formation mudstone in the hanging wall), reaches the surface near the southern edge of the mountain front (Figure 3). The surface trace of the fault dies out ~1 km east of the city of Piru, near the mouth of Piru Creek. The mechanical connection between the San Cayetano fault and the Santa Susana fault--the major, high-slip-rate north-dipping reverse fault to the east – is structurally complicated, and there does not appear to be a simple, through-going mechanical connection between these two faults (Yeats, 1987; Huftile and Yeats, 1996). -
Seismotectonics of the Zagros (Iran) from Orogen-Wide Earthquake Relocations
Final Project Report, NSF Award 1524815 Seismotectonics of the Zagros (Iran) from orogen-wide earthquake relocations Edwin Nissen1;2 & Ezgi Karas¨ozen2 1 School of Earth and Ocean Sciences, University of Victoria, Victoria, BC, Canada 2 Department of Geophysics, Colorado School of Mines, Golden, CO 03/15/2016{02/28/2019 Note: this final report is modifed and abridged from our recent paper: Karas¨ozen,E., Nissen, E., Bergman, E. A., and Ghods, A. (2019). Seismotectonics of the Zagros (Iran) From Orogen-Wide, Calibrated Earthquake Relocations. Journal of Geophysical Research: Solid Earth, https://doi.org/10.1029/2019JB017336. This related paper was also supported directly through this NSF award: Nissen, E., Ghods, A., Karas¨ozen,E., Elliott, J. R., Barnhart, W. D., Bergman, E. A., Hayes, G. P., Jamal-Reyhani, M., Nemati, M., Tan, F., Abdulnaby, W., Benz, H. M., Shahvar, M. P., Talebian, M., and Chen, L. (2019). The 12 November 2017 Mw 7.3 Ezgeleh-Sarpolzahab (Iran) earthquake and active tectonics of the Lurestan arc. Journal of Geophysical Research: Solid Earth, 124, 2124-2152. Summary We use calibrated earthquake relocations to reassess the distribution and kinematics of faulting in the Zagros range, southwestern Iran. This is amongst the most seismically-active fold-and- thrust belts globally, but knowledge of its active faulting is hampered by large errors in reported epicenters and controversy over earthquake depths. Mapped coseismic surface faulting is extremely rare, with most seismicity occurring on blind reverse faults buried beneath or within a thick, folded sedimentary cover. Therefore, the distribution of earthquakes provides vital information about the location of active faulting at depth. -
Nazca Plate Region) GRENADA 80°W 60°W 40°W 11900900 a A' 1 1 1 2 0 200 400 600 800 1,000 1,200 BARBADOS Compiled by Gavin P
U.S. DEPARTMENT OF THE INTERIOR OPEN-FILE REPORT 2015–1031-E U.S. GEOLOGICAL SURVEY This report supplements Open-File Report 2010–1083-E 80°W 70°W 60°W 50°W PRE-INSTRUMENTAL SEISMICITY 1500 – 1899 SAINT LUCIA Seismicity of the Earth 1900–2013 BARBADOS Deaths, tsunami, MMI VIII+, or M 8 SAINT VINCENT AND THE GRENADINES HONDURAS M 8.5 labeled with year ARUBA CURAÇAO Seismotectonics of South America (Nazca Plate Region) GRENADA 80°W 60°W 40°W 11900900 A A' 1 1 1 2 0 200 400 600 800 1,000 1,200 BARBADOS Compiled by Gavin P. Hayes, Gregory M. Smoczyk, Harley M. Benz, Antonio Villaseñor, TRINIDAD AND TOBAGO CURAÇAO NICARAGUA Barranquilla Maracaibo Caracas HONDURAS GRENADA 3 Valencia Maracay Demerara Plain and Kevin P. Furlong Cartagena TRENCH AXIS Managua Barquisimeto NICARAGUA 19921992 0 2014 11950950 Clark Basin 10° COSTA RICA PANAMA 1U.S. Geological Survey VENEZUELA 2 GUYANA Institute of Earth Sciences, Consejo Superior de Investigaciones Científicas, (CSIC), Barcelona, Spain COSTA RICA Panama FRENCH 3Department of Geosciences, Pennsylvania State University, University Park, Pa., USA San Jose Cucuta VENEZUELA SURINAME GUIANA 10°N 11983983 PANAMA –200 COLOMBIA Bucaramanga TECTONIC SUMMARY 19341934 GUYANA Equator The South American arc extends over 7,000 kilometers (km), from the Chilean margin triple junction offshore of southern Chile, to Medellin Equator ECUADOR its intersection with the Panama fracture zone, offshore of the southern coast of Panama in Central America. It marks the plate –400 Manizales FRENCH boundary between the subducting Nazca plate and the South America plate, where the oceanic crust and lithosphere of the Nazca Bogota SURINAME PROFILE A plate begin their descent into the mantle beneath South America. -
Pdf/17/3/932/5319294/932.Pdf 932 by Guest on 28 September 2021 Research Paper
Research Paper GEOSPHERE Late Pleistocene rates of rock uplift and faulting at the boundary between the southern Coast Ranges and the western Transverse GEOSPHERE, v. 17 no. 3 Ranges in California from reconstruction and luminescence dating https://doi.org/10.1130/GES02274.1 14 figures; 2 tables of the Orcutt Formation CORRESPONDENCE: [email protected] Ian S. McGregor and Nathan W. Onderdonk Department of Geological Sciences, California State University–Long Beach, 1250 Bellflower Boulevard, Long Beach, California 90804, USA CITATION: McGregor, I.S., and Onderdonk, N.W., 2021, Late Pleistocene rates of rock uplift and faulting at the boundary between the southern Coast Ranges ABSTRACT consistent with models that attribute shortening across the Santa Maria Basin and the western Transverse Ranges in California from to accommodation of clockwise rotation of the western Transverse Ranges and reconstruction and luminescence dating of the Orcutt Formation: Geosphere, v. 17, no. 3, p. 932–956, https:// The western Transverse Ranges and southern Coast Ranges of California suggest that rotation has continued into late Quaternary time. doi .org /10.1130 /GES02274.1. are lithologically similar but have very different styles and rates of Quaternary deformation. The western Transverse Ranges are deformed by west-trending Science Editor: Andrea Hampel folds and reverse faults with fast rates of Quaternary fault slip (1–11 mm/yr) ■ INTRODUCTION Associate Editor: Jeff Lee and uplift (1–7 mm/yr). The southern Coast Ranges, however, are primarily deformed by northwest-trending folds and right-lateral strike-slip faults with The Coast Ranges of California are deformed by northwest-striking faults Received 15 April 2020 Revision received 16 November 2020 much slower slip rates (3 mm/yr or less) and uplift rates (<1 mm/yr). -
U.S. Geological Survey Final Technical Report Award No
U.S. Geological Survey Final Technical Report Award No. G12AP20066 Recipient: University of California at Santa Barbara Mapping the 3D Geometry of Active Faults in Southern California Craig Nicholson1, Andreas Plesch2, John Shaw2 & Egill Hauksson3 1Marine Science Institute, UC Santa Barbara 2Department of Earth & Planetary Sciences, Harvard University 3Seismological Laboratory, California Institute of Technology Principal Investigator: Craig Nicholson Marine Science Institute, University of California MC 6150, Santa Barbara, CA 93106-6150 phone: 805-893-8384; fax: 805-893-8062; email: [email protected] 01 April 2012 - 31 March 2013 Research supported by the U.S. Geological Survey (USGS), Department of the Interior, under USGS Award No. G12AP20066. The views and conclusions contained in this document are those of the authors, and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U.S. Government. 1 Mapping the 3D Geometry of Active Faults in Southern California Abstract Accurate assessment of the seismic hazard in southern California requires an accurate and complete description of the active faults in three dimensions. Dynamic rupture behavior, realistic rupture scenarios, fault segmentation, and the accurate prediction of fault interactions and strong ground motion all strongly depend on the location, sense of slip, and 3D geometry of these active fault surfaces. Comprehensive and improved catalogs of relocated earthquakes for southern California are now available for detailed analysis. These catalogs comprise over 500,000 revised earthquake hypocenters, and nearly 200,000 well-determined earthquake focal mechanisms since 1981. These extensive catalogs need to be carefully examined and analyzed, not only for the accuracy and resolution of the earthquake hypocenters, but also for kinematic consistency of the spatial pattern of fault slip and the orientation of 3D fault surfaces at seismogenic depths.