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White Mountains
The Ediacaran–Cambrian transition in the southern Great Basin, United States
Onset of long-lived silicic and alkaline magmatism in eastern North America preceded Central Atlantic Magmatic Province emplacement
Seismic and Geodetic Analysis of Rupture Characteristics of the 2020 M w 6.5 Monte Cristo Range, Nevada, Earthquake
Topaz in New Hampshire's White Mountains
INCREASE IN CARBONATE CONTRIBUTION FROM FRAMEWORK-BUILDING METAZOANS THROUGH EARLY CAMBRIAN REEFS OF THE WESTERN BASIN AND RANGE, USA
Late Cretaceous unroofing of the White Mountains, New Hampshire, USA: An episode of passive margin rejuvenation?
Detrital zircon geochronology of Neoproterozoic–Lower Cambrian passive-margin strata of the White-Inyo Range, east-central California: Implications for the Mojave–Snow Lake fault hypothesis
Vertical zonation of the Barcroft granodiorite, White Mountains, California: Implications for magmatic processes
The role of low-angle normal faulting in active tectonics of the northern Owens Valley, California
Delineating a road-salt plume in lakebed sediments using electrical resistivity, piezometers, and seepage meters at Mirror Lake, New Hampshire, U.S.A
Rates of extension along the Fish Lake Valley fault and transtensional deformation in the Eastern California shear zone–Walker Lane belt
Cenozoic volcanism and tectonics in the Queen Valley area, Esmeralda County, western Nevada
The Queen Valley pull-apart basin is located at the northern extent of the White Mountains in western Nevada. The basin is bounded to the south by the NE-trending Queen Valley fault zone and to the north by the E-W–trending Coaldale fault zone. The curvilinear trace of the Queen Valley normal fault extends ~16 km northeast from the northern termination of the Owens Valley–White Mountain fault zone to the western Coaldale fault system. Using new (U-Th)/He and 40 Ar/ 39 Ar geochronology, fault kinematic data, and detailed geologic mapping (1:10,000), this study documents a three-stage late Tertiary tectonic evolution of the eastern Queen Valley area and defines the role of the Queen Valley fault system as an integral part of the right-lateral transtensional Walker Lane belt. The Queen Valley area was affected by an ignim-brite flare-up in Utah, Nevada, and California, as recorded by late Oligocene rhyolites (ca. 26 Ma). The eruption of these widespread ash flows was accompanied locally by extension, creating a series of ENE-trending half grabens. The faults are sealed by Miocene andesite (ca. 12 Ma), constraining the timing of extension to late Oligo-cene or early Miocene. Mid-Miocene Basin and Range extension produced E-dipping normal fault systems in the Yerington area to the north and W-dipping normal faults in the White Mountains to the south. Displacement between these fault systems with opposite polarity was accommodated by a series of right-lateral faults in the Queen Valley area. A change in extension direction from E-W extension to NW-SE during the Pliocene resulted in a transition to transcurrent and transtensional structures in the central Walker Lane belt. The beginning of transtension on the east side of the White Mountains was marked by the opening of the Fish Lake Valley pull-apart basin at ca. 6 Ma, as constrained by Upper Miocene volcanic units. Similarly, the Queen Valley pull-apart basin was a product of the reactivation of the White Mountain–Owens Valley fault zone as a right-lateral fault ca. 3 Ma, based on thermochronological data and offset Pliocene basaltic andesite (ca. 3.1 Ma) along the Queen Valley fault.
Deformation of the late Miocene to Pliocene Inyo Surface, eastern Sierra region, California
A middle and late Miocene erosion surface, the Inyo Surface, underlies late Miocene mafic flows in the White Mountains and late Miocene and (or) early Pliocene flows elsewhere in the eastern Sierra region. The Inyo Surface is correlated with an erosion surface that underlies late Miocene mafic flows in the central and northern Sierra Nevada. The mafic flows had outpourings similar to flood basalts, although of smaller volume, providing paleohorizontal and paleolowland indicators. The flows filled and locally topped the existing landscape forming broad plateau-like flats. Topographic relief in the region was characterized by weathered and rounded slopes prior to late Miocene mafic magmatism. Relicts of the older landscape lie adjacent to late Miocene and early Pliocene basalt-covered lowlands that now occur within the crests of ranges that have 2500–3000 m relief and dramatically steep escarpments. Late Miocene mafic flows that lie on the crest of the Sierra Nevada adjacent to the White Mountains predate significant activity on the Sierra Nevada frontal fault zone. These deposits and accompanying erosion surfaces provide excellent strain markers for reconstructing part of the Walker Lane north of the Garlock fault and west of the Amargosa drainage, here referred to as the eastern Sierra region. The Inyo Surface is a compound erosional surface that records at least four major erosion events during the Cenozoic. These four surfaces were first recognized on the Kern Plateau and named from oldest to youngest, the Summit Upland, the Subsummit Plateau, the Chagoopa Plateau, and the Canyon. The three older surfaces have also been subsequently modified by Pleistocene glaciation. The compound erosion surface, which is locally overlain by late Miocene mafic flows in the northern and central Sierra Nevada, is here referred to as the Lindgren Surface. Correlatives in the eastern Sierra region are found in the White Mountains, Inyo Mountains, Darwin Plateau, Coso Range, and nearby ranges.
Quaternary faulting in Queen Valley, California-Nevada: Implications for kinematics of fault-slip transfer in the eastern California shear zone–Walker Lane belt
Analysis of the strikes of 3841 dikes in 47 domains in the 500-km-long Late Jurassic Independence dike swarm indicates a distribution that is skewed clockwise from the dominant northwest strike. Independence dike swarm azimuths tend to cluster near 325° ± 30°, consistent with initial subparallel intrusion along much of the swarm. Dike azimuths in a quarter of the domains vary widely from the dominant trend. In domains in the essentially unrotated Sierra Nevada block, mean dike azimuths range mostly between 300° and 320°, with the exception of Mount Goddard (247°). Mean dike azimuths in domains in the Basin and Range Province in the Argus, Inyo, and White Mountains areas range from 291° to 354°; the mean is 004° in the El Paso Mountains. In the Mojave Desert, mean dike azimuths range from 318° to 023°, and in the eastern Transverse Ranges, they range from 316° to 051°. Restoration for late Cenozoic vertical-axis rotations, suggested by paleodeclinations determined from published studies from nearby Miocene and younger rocks, shifts dike azimuths into better agreement with azimuths measured in the tectonically stable Sierra Nevada. This confirms that vertical-axis tectonic rotations explain some of the dispersion in orientation, especially in the Mojave Desert and eastern Transverse Ranges, and that the dike orientations can be a useful if imperfect guide to tectonic rotations where paleomagnetic data do not exist. Large deviations from the main trend of the swarm may reflect (1) clockwise rotations for which there is no paleomagnetic evidence available, (2) dike intrusions of other ages, (3) crack filling at angles oblique or perpendicular to the main swarm, (4) pre-Miocene rotations, or (5) unrecognized domain boundaries between dike localities and sites with paleomagnetic determinations.
In situ oxygen isotope analysis of monazite as a monitor of fluid infiltration during contact metamorphism: Birch Creek Pluton aureole, White Mountains, eastern California
A geologic map represents the melding of field observations with various types of analytical data and earth science concepts. Choosing features to be portrayed is a reflection of the questions posed. Some would claim that in the mapping process, theory meets reality. However, a map is a more subjective product based on the sum of the geologist's prior training, aggregate field experience, and the stage of development of scientific concepts, the complexity of the mapped units, the extent and quality of exposures, the wealth of constraining ancillary data, and the time and thought expended in the mapping. The published map also reflects accommodations to the scientific reviewers' knowledge, and to technical compromises required by the printer-publisher. Because mapping style depends on a geologist's prior experience, it is necessarily a somewhat idiosyncratic process. My own field research has focused chiefly on the petrologic-structural development of Mesozoic and younger contractional orogenic belts, and through them, the tectonic evolution of continental margins. Mapping has been an essential step enhancing my understanding of processes that have shaped convergent portions of Earth's crust. (1) For instance, field relations combined with mineralogic analysis in the Panoche Pass area, southern Diablo Range, central California, indicated relatively high pressure–low temperature recrystallization and postmetamorphic, low-angle faulting of the Franciscan Complex. (2) Mapping of a similar Franciscan terrane in the central Diablo Range identified imbricate, subhorizontal, syn- to postmetamorphic bedding-plane thrust faults and implied accretionary growth in the Pacheco Pass quadrangle. (3) Field study of a structural inversion of high-grade metamorphic rocks tectonically overlying low-grade equivalents in the Sanbagawa belt, central Shikoku, Japan, led to the interpretation of postrecrystallization, ductile nappe emplacement and, as in California and the Western and Eastern Alps, (4) a progressive, relatively high P –low T metamorphism-exhumation subduction-zone model. (5) Mapping the interstratified distal turbidites and mafic lavas, and the discovery of pillow tops in the Sawyers Bar area, documented in situ stages of oceanic-island arc development in the North Fork terrane, central Klamath Mountains, northwestern California. Bulk-rock compositions of interlayered ocean-island basalts and island-arc tholeiites supported this interpretation. (6) Detailed geologic mapping combined with remote sensing in the central White Mountains, easternmost California, demonstrated that the Middle Jurassic Barcroft granodioritic complex is a steeply southeast-dipping slab that intruded previously deformed mid-Mesozoic arc volcanic rocks and Neoproterozoic–Lower Cambrian platform strata along a high-angle reverse fault. Conclusions derived from these studies, as well as more general plate-tectonic syntheses, depended on geologic mapping, and, for me, the field mapping was an enjoyable and scientifically fulfilling experience.
Abstract This field guide was created in coordination with the Geological Society of America Field Forum “Rethinking the Assembly and Evolution of Plutons: Field Tests and Perspectives,” held 7-14 October 2005 in the Sierra Nevada and White and Inyo ranges, California. The goal of this five-day field trip was to examine field relations and characteristics of plutons in the central Sierra Nevada and in the White and Inyo ranges as they relate to processes of pluton growth and emplacement and, more particularly, as they relate to the hypothesis that plutons are assembled slowly and incrementally.