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The Role of Low-Angle Normal Faulting in Active Tectonics of the Northern Owens Valley, California

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The Role of Low-Angle Normal Faulting in Active Tectonics of the Northern Owens Valley, California The role of low-angle normal faulting in active tectonics of the northern Owens Valley, California Fred M. Phillips and Lisa Majkowski DEPARTMENT OF EARTH AND ENVIRONMENTAL SCIENCE, NEW MEXICO TECH, SOCORRO, NEW MEXICO 87801, USA ABSTRACT The Owens Valley of eastern California is an extensional graben. The mechanics of extension have traditionally been explained by means of high-angle normal faulting. However, this mechanism appears to be inconsistent with both the accepted tectonic structures of associated basins and with the expected kinematics of regional extension. We have therefore reexamined several lines of evidence that bear on the fault structures bounding the northern Owens Valley. Examination of fault-outcrop geometry indicates that valley-bounding fault planes dip between 26° and ~90°. Measurement of numerous fault planes that dip between 25° and 35° demonstrates that low-angle faulting must play an important role in the extensional process. We examined the alluvial fan/drainage basin area ratio of alluvial fans along the west slope of the White Mountains. These vary between ~1.00 and 0.05. The larger area ratios are associated with low-angle mountain-front faults, and the smaller ratios are associated with high-angle faults. The Bishop tuff, both in outcrop and in subcrop, shows obvious anticlinal rollovers as the tuff sheet approaches the bounding faults, which may indicate listric faulting geometry. Relocated earthquake hypocenter data defi ne a west-dipping band of seismicity at 4–7 km depth beneath the Owens Valley. Fault-plane solutions for these events permit low-angle westward-directed slip. These observations indicate that the traditional high-angle normal faulting model is inadequate. More plausible alternative structures include low-angle planar normal bounding faults and faulting controlled by either east-dipping or west-dipping master detachment faults. LITHOSPHERE; v. 3; no. 1; p. 22–36. doi: 10.1130/L73.1 INTRODUCTION the surfi cial neotectonic features there rooted Finally, seismic hazard analyses also require in low-angle structures similar to the Miocene assumptions regarding fault geometry. A bet- The Great Basin constitutes a continental- ones to the east, or is the geometry of faulting ter understanding of fault geometry may help scale topographic and hydrologic feature cre- instead “steep and fairly penetrating,” as postu- to improve hazard estimates, and such insights ated by extensional tectonics. Extension began lated by Wernicke et al. (1988, p. 1751)? may be transferable to other portions of the during the Miocene in the central Great Basin, A second reason to study the mechanics of Basin and Range Province. but at present, most of the tectonic activity is extension in this area is to investigate a discrep- concentrated on the western and eastern mar- ancy between contemporary geodetic estimates STUDY AREA gins of the region (Wernicke, 1992). The west- of displacement rate and rates inferred over geo- ern margin is particularly active. The mechanics logical time scales based on fault investigations. The Owens Valley defi nes the western mar- of extension in this region are of interest for sev- The geodetically based rates are quite high. gin of the Great Basin and the eastern margin eral reasons. One reason is to help understand Geodetic measurements indicate that at the of the Sierra Nevada block (Fig. 1). The valley the continuity, or lack thereof, between tectonic latitude of the northern Owens Valley, approxi- consists of a trough-like structure, 140 km in mechanisms in the highly extended terrain of the mately two-thirds of the total extension between length and 25–10 km in width, striking 30° to Las Vegas–Death Valley area (in considerable the North American craton and the Pacifi c plate 20° west of north. Along most of its length, the part accomplished during the Miocene) and the is concentrated in a zone of only 70 km between western side of the valley is formed by the dra- more limited Pliocene–Quaternary extension the Sierra Nevada crest and Fish Lake Valley matic eastern escarpment of the Sierra Nevada, directly east of the Sierra Nevada block. Due to (Dixon et al., 2000). However, in a comparison with total relief varying from 1700 to 2700 m. a long interval of extension and erosion, deep- of geodetic and geological displacement rates The eastern side is formed by the White and seated low-angle structures are well exposed in, using a kinematic block model, the modeled Inyo Mountains, which are more gentle than for example, the Las Vegas area, Death Valley, rates based on geodetic data are two to fi ve the Sierra Nevada and which have crests gener- and Panamint Valley (Wernicke et al., 1988). times larger than the ones based on fi eld stud- ally rising 1500–1000 m above the valley fl oor, In contrast, along the highly active southwest- ies of faults (McCaffrey, 2005). The fault-based but which extend up to 2700 m above the val- ern boundary of the Great Basin, the struc- rates necessarily involve assumptions regard- ley fl oor in the northern portion of the White tures facilitating extension are generally buried ing fault geometry, and thus elucidation of fault Mountains. This generally north-south–ori- beneath subsiding and aggrading basins. Are structures may shed light on this discrepancy. ented graben-like structure is typical of valleys Editor’s note: This article is part of a special issue devoted to the GSA Field Forum titled Structure and Neotectonic Evolution of Northern Owens Valley and the Volcanic Tableland, California, convened by David A. Ferrill, Southwest Research Institute, Alan P. Morris, Southwest Research Institute, and Nancye H. Dawers, Tulane University. More papers on this subject will follow in subsequent issues, and these will be collected online at http://lithosphere.gsapubs.org/ (click on Themed Issues). 22 For permission to copy, contact [email protected] | |Volume © 2011 3 Geological | Number Society1 | LITHOSPHERE of America Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/3/1/22/3044243/22.pdf by guest on 27 September 2021 Reevaluation of fault geometry in the northern Owens Valley, California | RESEARCH 118°45′0″W 118°20′0″W Montgomery Creek Morris Creek White Marble Creek Mountains Study Queen Dicks Canyon area Falls Canyon Rock Creek Middle Canyon Birch Creek Hammil Valley Lone Tree Creek Milner Creek Sabies Canyon Straight Canyon Chalfant Valley Piute Creek 37°30′0″N Wheeler Crest 37°30′0″N Coldwater Canyon RVF FSF Volcanic Tableland Gunter Creek Pine Creek Silver Canyon Mount Tom Round Legend Valley Faults Mountain down Bishop WMFZ Oblique Basin Mtn Strike slip Poleta Canyon Valley down Undifferentiated Drainage basins Alluvial fans Basin Depth (km) 0–0.05 0.05–0.2 0.2–0.5 Mount Humphreys 0.5–1 N Black Canyon Coyote Warp 1–2 2–3 3–4 OVRO 4–5 5–6 6–7 Big Pine 7–21.28 OVFZ 37°5′0″N 37°5′0″N 118°45′0″W 118°20′0″W Figure 1. Tectonic geology of the northern Owens Valley. Faults are from Bryant (2005) and from mapping by the authors. RVF—Round Valley fault, WMFZ—White Mountain fault zone, FSF—Fish Slough fault, OVFZ—Owens Valley fault zone. OVRO—Owens Valley Radio Observatory. Color contours are depth to basement from gravity-data inversion by Saltus and Jachens (1995). Yellow arrows represent the direction of fault-plane dips obtained from three-point solutions on scarps or other fault-related geomorphic features (see Table 1); the numbers in the arrows are the dip value in degrees. Additional numbers in italics are dips obtained from inclinometer measurements on fault-plane exposures. For faults with steep dip solutions, double- headed arrows are shown. Inasmuch as the dip orientation estimates are not robust, the preferred dip direction is indicated by a black triangle on the end of one of the arrows. Arrows along the White Mountains fault zone have been shifted east of the point of measurement to avoid obscuring other data. The red circles represent the fan/drainage basin area ratios of alluvial fans along the western side of the White Mountains (see Table 2 for data). Selected fans and associated drainage basins are highlighted. LITHOSPHERE | Volume 3 | Number 1 | www.gsapubs.org 23 Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/3/1/22/3044243/22.pdf by guest on 27 September 2021 PHILLIPS AND MAJKOWSKI in the Great Basin to the east. The mechanics continental boundary to the west changed to a faulted continuation of this valley fl oor, indicat- of tectonics in the northern Owens Valley since subduction zone. Throughout the Mesozoic, arc ing that Miocene faulting may have been toward 760 ka can be traced by evaluation of the defor- volcanism dominated, and coalescence of plu- the eastern side of the present Owens Valley. At mation of the Bishop tuff, created by the erup- tons under that arc created the Sierra Nevada that time, extension was directed approximately tion of Long Valley caldera. Batholith. Today, the Inyo and White Moun- east-west (Wernicke and Snow, 1998; McQuar- The Owens Valley is clearly a tectonically tains that bound the Owens Valley on the east rie and Wernicke, 2005), and thus normal fault- produced feature, and its structural characteris- are dominated by Paleozoic sedimentary rock, ing was initiated along an approximately north- tics have largely been a matter of consensus for while the Sierra Nevada range to the west has south strike. the past 140 yr. It is bounded on the west side by mostly been eroded down to the granitic rocks Middle to late Neogene cooling ages in the the Sierra Nevada frontal fault and on the east of the batholith (Bateman and Wahrhaftig, Owens Valley region exhibit a distinctly bimodal by the White Mountains fault zone and the Inyo 1966; Saleeby, 1999).
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