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Systematic Variation of Late Pleistocene Fault Scarp Height in the Teton Range, Wyoming, USA: Variable Fault Slip Rates Or Variable GEOSPHERE; V

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Systematic Variation of Late Pleistocene Fault Scarp Height in the Teton Range, Wyoming, USA: Variable Fault Slip Rates Or Variable GEOSPHERE; V Research Paper THEMED ISSUE: Cenozoic Tectonics, Magmatism, and Stratigraphy of the Snake River Plain–Yellowstone Region and Adjacent Areas GEOSPHERE Systematic variation of Late Pleistocene fault scarp height in the Teton Range, Wyoming, USA: Variable fault slip rates or variable GEOSPHERE; v. 13, no. 2 landform ages? doi:10.1130/GES01320.1 Glenn D. Thackray and Amie E. Staley* 8 figures; 1 supplemental file Department of Geosciences, Idaho State University, 921 South 8th Avenue, Pocatello, Idaho 83209, USA CORRESPONDENCE: thacglen@ isu .edu ABSTRACT ously and repeatedly to climate shifts in multiple valleys, they create multi­ CITATION: Thackray, G.D., and Staley, A.E., 2017, ple isochronous markers for evaluation of spatial and temporal variation of Systematic variation of Late Pleistocene fault scarp height in the Teton Range, Wyoming, USA: Variable Fault scarps of strongly varying height cut glacial and alluvial sequences fault motion (Gillespie and Molnar, 1995; McCalpin, 1996; Howle et al., 2012; fault slip rates or variable landform ages?: Geosphere, mantling the faulted front of the Teton Range (western USA). Scarp heights Thackray et al., 2013). v. 13, no. 2, p. 287–300, doi:10.1130/GES01320.1. vary from 11.2 to 37.6 m and are systematically higher on geomorphically older In some cases, faults of known slip rate can also be used to evaluate ages landforms. Fault scarps cutting a deglacial surface, known from cosmogenic of glacial and alluvial sequences. However, this process is hampered by spatial Received 26 January 2016 Revision received 22 November 2016 radionuclide exposure dating to immediately postdate 14.7 ± 1.1 ka, average and temporal variability of offset along individual faults and fault segments Accepted 13 January 2017 12.0 m in height, and yield an average postglacial offset rate of 0.82 ± 0.13 (e.g., Z. Lifton et al., 2015; Pierce and Morgan, 1992) and can lead to erroneous Published online 24 February 2017 m/k.y. using simple scarp height (average 11.2 m, offset rate 0.76 ± 0.11 m/k.y. interpretations (Gillespie and Molnar, 1995). using vertical separation). We apply the offset rate to higher fault scarps to de- Fault activity in glaciated areas may also be complicated by influences velop preliminary age estimates for the geomorphically older landforms, with of deglacial unloading and meltwater release and infiltration (e.g., Hampel an initial assumption of constant offset rate through time. The landform age et al., 2007). These processes can influence fault slip rates during the deglacial estimates of 16.2 ± 3.9 ka to 45.9 ± 11.0 ka imply that glaciation and alluviation period, confounding studies that focus exclusively on deglacial and postglacial influenced the range front during marine isotope stages 2 and 3. However, landforms. fault offset rate variability, suggested by previous work to be attributable to Understanding fault offset rates is often limited by sparse glacial and allu­ Yellowstone ice cap deglacial processes, suggests that the fault scarp height vial chronologies. In many locations, the chronology includes only a single pattern might also be interpreted as a reflection of strongly variable offset advance, typically an advance correlative with the last glacial maximum (LGM, rates in landforms of only slightly contrasting age. These results demonstrate 26–18 ka; Mix et al., 2001) or deglacial events, rendering difficult the evaluation the need for detailed geochronology of isochronous landforms and sediments of temporal fault slip variability. This question is particularly relevant in regions of multiple ages, in order to understand both faulting and glaciation on faulted with complex glacial histories spanning the last glacial cycle. For example, range fronts. glacial chronologies document prominent advances during marine isotope stages (MIS) 4 and/or 3 (71–57 ka and 57–29 ka; age ranges from Lisiecki and INTRODUCTION Raymo, 2005) in addition to MIS 2 (29–14 ka) in Central Asia (Rother et al., 2014), New Zealand (Shulmeister et al., 2010; Putnam et al., 2013), southern Glacial and alluvial sequences mantling mountain range fronts frequently South America (Darvill et al., 2015), western North America (e.g., Thackray, host scarps of active faults and are used to evaluate spatial and temporal vari­ 2001; see following discussion), and elsewhere. Longer glacial chronologies, ation of fault motion (e.g., McCalpin, 1996, in New Zealand; Scott et al., 1983, with multiple events separated by 10 k.y. or more, allow analysis of longer on the Wasatch fault, Utah; Ansberque et al., 2016, in Tibet). Glacial and alluvial term fault behavior and, potentially, the use of fault offset rates to hypothesize sequences provide geomorphic and stratigraphic markers that are typically ages of earlier glacial events. amenable to radiocarbon, luminescence, and cosmogenic exposure dating This project, focusing on the Teton fault, uses a base of published cosmo­ (e.g., Chen et al., 2012; Kenworthy et al., 2014; Licciardi and Pierce, 2008). Be­ genic radionuclide (CRN) glacial chronologic data (Licciardi and Pierce, 2008), cause glacial and alluvial sequences in the ranges often respond simultane­ coupled with high­quality lidar (light detection and ranging) topographic data (Teton National Park, 2014; Teton Conservation District, 2008; EarthScope Inter­ For permission to copy, contact Copyright *Current address: Minnesota Geological Survey, 2609 Territorial Road, St. Paul, Minnesota mountain Seismic Belt LiDAR Project, 2008), to reveal probable variability of Permissions, GSA, or [email protected]. 55114, USA glacial landform ages and fault offset rates in time and space. Our study re­ © 2017 Geological Society of America GEOSPHERE | Volume 13 | Number 2 Thackray and Staley | Variation of Teton Range fault scarp height Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/13/2/287/1000929/287.pdf 287 by guest on 02 October 2021 Research Paper veals challenges with using glacial chronologies, which are typically incom­ 110°50′0″W110°40′0″W110°30′0″W110°20′0″W plete, for understanding fault offsets. The project also reveals new understand­ ing of this major fault of the Yellowstone–Snake River Plain region, in which normal faulting and volcanism, influenced by migration of the Yellowstone volcanic field, dominate the Neogene and Quaternary geologic history (e.g., Pierce and Morgan, 1992). The project develops the best possible postglacial 43°50′0″N Teton 43°50′0″N fault offset rate, given current knowledge of fault scarp topography and glacial Range geochronology, points to gaps in our understanding of the fault’s mechanisms and hazards, and suggests the types of data that are needed to understand this and other faults more fully. In particular, the Teton Range front is an ideal setting in which to examine the effects of advance and retreat of glacial ice on fault slip rates. Our results also point to possible pre­LGM mountain glacier advances not yet documented in the CRN chronologies, as well as the poten­ 43°40′0″N 43°40′0″N tial impacts of fault motion on glacial landform preservation. These findings inform the study of faulting in a variety of landscapes influenced by episodic glacial and alluvial deposition. Jackson Hole BACKGROUND Setting 43°30′0″N 43°30′0″N The Teton Range (Fig. 1) is in the northeastern Basin and Range province. The range exposes Archean metasedimentary rocks and Archean and Protero­ zoic intrusive igneous rocks, overlain unconformably by west­dipping Paleozoic sedimentary and Quaternary volcanic rocks (Love et al., 1992). The Teton fault is a N10°E­striking, east­dipping normal fault that separates the Teton Range from Jackson Hole. The fault has undergone 2.5–3.5 km of slip over the past 2–3 m.y. 43°20′0″N 43°20′0″N (Byrd et al., 1994), raising preexisting topography to form the highest eleva­ tions in the region. The Teton fault represents an anomaly among faults in the Snake River Plain–Yellowstone region. Surface scarps cutting Late Pleistocene glacial landforms are higher (12–36 m) and inferred fault offset rates greater (to 2.4 m/k.y.; Byrd, 1995) than along other regional normal fault systems. The 110°50′0″W110°40′0″W 110°30′0″W110°20′0″W Lost River fault in central Idaho, for example, displays scarps of 2–15 m in Late Pleistocene glacial and glacial­fluvial landforms (Staley, 2015) and yields Figure 1. Geomorphic, glacial, and geologic context of study area. Thick line shows fault scarps trench­based slip rates of 0.18–0.3 mm/yr (Haller and Wheeler, 2010). Scarps mapped through interpretation of lidar (light detection and ranging) data. Pinedale 1–3 and Bull Lake moraines were constructed by the Yellowstone ice cap outlet glacier. The outlet glacier of the Sawtooth fault are 4–9 m high in Late Pleistocene landforms and yield filled Jackson Hole during the Bull Lake glaciation (marine isotope stage, MIS 6), but terminated scarp­derived slip rates of 0.5–0.9 m/k.y. (Thackray et al., 2013). The height and at the northern edge of the study area during the Pinedale glaciation (MIS 2). Ice cap limits are variability of Teton fault scarps reflect older glacial landforms, very rapid offset from Licciardi and Pierce (2008). Small box shows the Taggart Lake area, a focus of this study. rates, and/or highly variable offset rates since the peak of the last glaciation. The Teton Range rises to 4200 m, 2400 m above Jackson Hole, the adja­ cent structural basin (Fig. 1). The Teton Range presents a major orographic the last two glaciations and imposed strong geomorphic effects on the basin barrier to moist westerly winds funneled along the eastern Snake River Plain, and adjacent range front. Mountain glaciers formed in the Teton Range and contributing to the relatively moist, montane climate (1500–2000 mm/yr) and expanded down several major valleys to cross the range front (Figs.
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