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Development of surface ruptures by hanging-wall extension over a thrust ramp along the Ragged Mountain fault, Katalla, Alaska, USA: Applications of high-resolution three-dimensional terrain models
Outcrops and well logs as a practicum for calibrating the accuracy of traveltime tomograms
Salt-dissolution faults versus tectonic faults from the case study of salt collapse in Spanish Valley, SE Utah (USA)
Plate margin deformation and active tectonics along the northern edge of the Yakutat Terrane in the Saint Elias Orogen, Alaska, and Yukon, Canada
Structure of the actively deforming fold-thrust belt of the St. Elias orogen with implications for glacial exhumation and three-dimensional tectonic processes
Structural relationships in the eastern syntaxis of the St. Elias orogen, Alaska
Application of LIDAR to resolving bedrock structure in areas of poor exposure: An example from the STEEP study area, southern Alaska
The Bering and Steller Glaciers of southern Alaska provide the opportunity to investigate relationships between climate and tectonics in a glaciated mountain belt. The glaciers profoundly impact the climate, ecology, and landscape of the northeastern Gulf of Alaska margin. The glaciers flow among and over deformed and eroded rocks of the Yakutat microplate, where geological structures impart topographic variations in the landscape that strongly affect glacier dynamics. The Bering Glacier flows along a tectonic boundary within the microplate that separates two regions of different structural style and history. East of the glacier, erosion of folded and thrust-faulted sedimentary strata creates E-W ridges and valleys oriented at high angle to ice flow. Farther west, second-phase folds and faults are superimposed on these structures, creating mountain blocks with complex structural geometry. Where the second-phase limbs have an E-W structural grain the glaciers flow around broad headlands, and meltwater streams discharge southward through narrow canyons. N to NE trending fold limbs are streamlined by glacial scouring parallel to folded bedding, and the elongated mountains are separated by narrow ice- and water-filled troughs, or flat-floored sediment-filled valleys. Measurements of ice motion and glacier surface topography are used in conjunction with geological mapping to constrain the location of the tectonic boundary beneath the Bering Glacier. The boundary is inferred to lie beneath the west-central terminus and extend up-glacier, passing west of the Grindle Hills and extending into the Khitrov Hills. The large volume of debris trapped in the Medial Moraine Band along the western edge of the Bering Glacier overlies a NNE-trending bedrock high formed by second-phase folding. The Bering and Steller Glaciers coalesce beneath the Medial Moraine Band, which then divides into several flows of faster and slower moving ice and debris. Thermokarst dominates the glacial structure on the lower part of the moraine band, where ice flow is 20 m/a or less. To the west, the Steller Glacier diverges into several lobes where it flows among remnants of second-phase folds. The tectonic boundary beneath the Bering Glacier is inferred to be a concealed thrust or oblique-slip thrust fault that rises from the Aleutian megathrust or subduction zone, juxtaposing the second-phase folded terrain against and over the E-trending fold belt beneath the glacier. There is no surface expression of the tectonic boundary because of intense erosion and transport of rock debris by the glacier and meltwater rivers. Trunk river channels beneath the Bering Glacier are presumably affected by remnant structures at its base, where NNE-trending ridges and sediment filled troughs are juxtaposed against E-trending topography oriented at high angle to ice flow. This change in basal topography and structure presumably constricts the basal drainage network opposite a sharp bend in the Khitrov Hills, where surging initiated in 1993. Episodic freezing or deformation by ice flow in this part of the drainage network may create elevated fluid pressure that triggers episodic surging.
Holocene Slip Rate for the Western Segment of the Castle Mountain Fault, Alaska
Deformation driven by subduction and microplate collision: Geodynamics of Cook Inlet basin, Alaska
Abstract The Wasatch fault is a 370-km-long zone of normal faulting that forms the eastern edge of the Basin and Range Province in Utah and southeastern Idaho. The fault zone is subdivided into ten segments that range from 30 to 60 km in length and are each capable of generating earthquakes of M ~7. For the five central segments, multiple surface-faulting earthquakes have occurred during the Holocene, and vertical slip rates are ~1 mm/yr. Recurrence intervals for the individual central segments range from ~1300 to 2500 yr. The fault poses a significant seismic hazard to the highly urbanized Wasatch Front in north-central Utah. The field localities described in this guide provide an overview of the surface and subsurface character of the Wasatch fault zone. Five field trip stops are located along the Nephi, Provo, and Salt Lake City segments. We will observe fault scarps on Quaternary deposits, which record tectonic displacements associated with Holocene earthquakes, and fault-zone rocks exhumed from depths in excess of 10 km that are hydrothermally altered and have evidence of brittle and ductile deformation. Specific topics of discussion include the nature of piedmont fault scarps; the use of paleoseismic trenching and fault-scarp geomorphology to infer earthquake timing, recurrence intervals, and fault slip rates; and the subsurface structure and rheology of the fault . Keywords : faulting, paleoseismology, neotectonics, earthquake geology.
Deformation during terrane accretion in the Saint Elias orogen, Alaska
A Methodology for Probabilistic Fault Displacement Hazard Analysis (PFDHA)
Potential seismic hazards and tectonics of the upper Cook Inlet basin, Alaska, based on analysis of Pliocene and younger deformation
Abstract During the period lasting from about 150 to 80 Ma, two contemporaneous but geographically distinct tectonic regimes dominated the Cordillera (Fig. 1). In the eastern part, the largely thin-skinned Cordilleran fold and thrust belt and a coeval foreland basin developed as Proterozoic, Paleozoic, and lower Mesozoic strata were contracted and emplaced eastward onto the platformal cover of the North American craton. In the western Cordillera, subduction of oceanic crust along the continental margin gave rise to the magmatic arc, forearc-basin deposits, and subduction complex that are preserved respectively in the Sierran batholithic belt, Great Valley Group, and Franciscan Complex. Upper Jurassic, Lower Cretaceous, and lower Upper Cretaceous rocks elsewhere in the western Cordillera, including Washington and southwestern California, reside in large composite terranes that may have been displaced northward with respect to continental North America on the order of 1, 000 km or more since about 80 Ma. This hypothesis, supported chiefly by paleomagnetic data, is definitely controversial.
Structure of a fault segment boundary in the Lost River fault zone, Idaho, and possible effect on the 1983 Borah Peak earthquake rupture
Analysis of mesoscopic structures in the Jurassic Twin Creek Formation reveals two major periods of deformation in the central Wasatch and westernmost Uinta Mountains during Late Cretaceous through early Eocene time. Spaced cleavage, extension veins, and tension gash bands developed early in the evolution of the Mount Raymond thrust fault and were subsequently folded around first-phase folds as deformation progressed. First-phase folds occur as trains of northeast-plunging, asymmetric anticlines and synclines, with an overall eastward vergence. A second spaced cleavage and associated extension veins and tension gash bands developed after the first-phase folding and prior to the development of second-phase folds. The first-phase and early second-phase structures were subsequently folded into east-northeast-trending second-phase anticlines and synclines during evolution of the Uinta arch. The Uinta arch in the central Wasatch and westernmost Uinta Mountains formed during Late Cretaceous to early Eocene time, partly in response to movement on the Hogsback thrust. Two possible models, which are consistent with the field data for the evolution of the Uinta arch, are (1) dextral wrench strain along the southern termination of the Hogsback thrust, and (2) dextral transpression along a south-dipping ramp where the Hogsback thrust cut down along the northern boundary of the basin in which the Middle Proterozoic Uinta Mountain Group was deposited.