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Published: 10 December 2022

Last updated: 28 January 2023

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1

Rickart, Eric A., Rebecca J. Rowe, Shannen L. Robson, Lois F. Alexander, and Duke S. Rogers. "Shrews of the Ruby Mountains, Northeastern Nevada." Southwestern Naturalist 56, no. 1 (March 2011): 95–102. http://dx.doi.org/10.1894/rts-08.1.

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2

Wanket, James A., David B. Wahl, and Jennifer E. Kusler. "Preliminary pollen record from Echo Lake, Ruby Mountains, Nevada." Quaternary International 387 (November 2015): 149. http://dx.doi.org/10.1016/j.quaint.2015.01.185.

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3

Thompson, Robert S. "Late Quaternary Environments in Ruby Valley, Nevada." Quaternary Research 37, no. 1 (January 1992): 1–15. http://dx.doi.org/10.1016/0033-5894(92)90002-z.

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AbstractPalynological data from sediment cores from the Ruby Marshes provide a record of environmental and climatic changes over the last 40,000 yr. The modern marsh waters are fresh, but no deeper than ∼3 m. A shallow saline lake occupied this basin during the middle Wisconsin, followed by fresh and perhaps deep waters by 18,000 to 15,000 yr B.P. No sediments were recovered for the period between 15,000 and 11,000 yr B.P., possibly due to lake desiccation. By 10,800 yr B.P. a fresh-water lake was again present, and deeper-than-modern conditions lasted until 6800 yr B.P. The middle Holocene was characterized by very shallow water, and perhaps complete desiccation. The marsh system deepened after 4700 yr B.P., and fresh-water conditions persisted until modern times. Vegetation changes in Ruby Valley were more gradual than those seen in the paleolimno-logical record. Sagebrush steppe was more widespread than at present through the late Pleistocene and early Holocene, giving way somewhat to expanded shadscale vegetation between 8500 and 6800 yr B.P. Shadscale steppe contracted by 4000 yr B.P., but had greater than modern coverage until 1000 to 500 yr ago. Pinyon-juniper woodland was established in the southern Ruby Mountains by 4700 yr B.P.

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4

Colgan, Joseph P., Keith A. Howard, Robert J. Fleck, and Joseph L. Wooden. "Rapid middle Miocene extension and unroofing of the southern Ruby Mountains, Nevada." Tectonics 29, no. 6 (December 2010): n/a. http://dx.doi.org/10.1029/2009tc002655.

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5

Schaefer, Vincent J. "Is something happening to our supply of Supercooled Clouds?" Journal of Weather Modification 10, no. 1 (April 3, 2018): 1–3. http://dx.doi.org/10.54782/jwm.v10i1.580.

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On October 19, 1977, on a flight from Albany, New York to Reno, Nevada, I spent most of the trip on the sunny side of the jet aircraft watching the world go by.... The flight route from Chicago to Reno went past Cheyenne, Elk Mountain, Flaming Gorge Reservoir, just north of the Bingham Copper Pit, and then across the Bonneville Salt Flats into Nevada. Much of the region west of Chicago was cloudless but shortly afterwe crossed the Nevada state line,the first batch of cumulus clouds appeared as we approached the Ruby Mountains. Proceeding west southwest, convective clouds increased in concentration until they obscured the ground. The sky above our plane was cloudless and therewere no middle clouds.....

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6

MacCready, Tyler, Arthur W. Snoke, James E. Wright, and Keith A. Howard. "Mid-crustal flow during Tertiary extension in the Ruby Mountains core complex, Nevada." Geological Society of America Bulletin 109, no. 12 (December 1997): 1576–94. http://dx.doi.org/10.1130/0016-7606(1997)109<1576:mcfdte>2.3.co;2.

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7

Wahl, David, Scott Starratt, Lysanna Anderson, Jennifer Kusler, Christopher Fuller, Elmira Wan, and Holly Olson. "A 7700 year record of paleoenvironmental change from Favre Lake, Ruby Mountains, Nevada." Quaternary International 387 (November 2015): 148–49. http://dx.doi.org/10.1016/j.quaint.2015.01.184.

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8

Lee, Sang-Yun, Calvin G. Barnes, Arthur W. Snoke, Keith A. Howard, and Carol D. Frost. "Petrogenesis of Mesozoic, Peraluminous Granites in the Lamoille Canyon Area, Ruby Mountains, Nevada, USA." Journal of Petrology 44, no. 4 (April 1, 2003): 713–32. http://dx.doi.org/10.1093/petrology/44.4.713.

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Abstract Two groups of closely associated, peraluminous, two-mica granitic gneiss were identified in the area. The older, sparsely distributed unit is equigranular (EG) with initial εNd ∼ − 8·8 and initial 87Sr/86Sr ∼0·7098. Its age is uncertain. The younger unit is Late Cretaceous (∼80 Ma), pegmatitic, and sillimanite-bearing (KPG), with εNd from −15·8 to −17·3 and initial 87Sr/86Sr from 0·7157 to 0·7198. The concentrations of Fe, Mg, Na, Ca, Sr, V, Zr, Zn and Hf are higher, and K, Rb and Th are lower in the EG. Major- and trace-element models indicate that the KPG was derived by muscovite dehydration melting (<35 km depth) of Neoproterozoic metapelitic rocks that are widespread in the eastern Great Basin. The models are broadly consistent with anatexis of crust tectonically thickened during the Sevier orogeny; no mantle mass or heat contribution was necessary. As such, this unit represents one crustal end-member of regional Late Cretaceous peraluminous granites. The EG was produced by biotite dehydration melting at greater depths, with garnet stable in the residue. The source of the EG was probably Paleoproterozoic metagraywacke. Because EG magmatism probably pre-dated Late Cretaceous crustal thickening, it required heat input from the mantle or from mantle-derived magma.

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9

Litherland, Mairi M., and Simon L. Klemperer. "Crustal structure of the Ruby Mountains metamorphic core complex, Nevada, from passive seismic imaging." Geosphere 13, no. 5 (August 25, 2017): 1506–23. http://dx.doi.org/10.1130/ges01472.1.

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10

HUDEC, MICHAEL R. "Mesozoic structural and metamorphic history of the central Ruby Mountains metamorphic core complex, Nevada." Geological Society of America Bulletin 104, no. 9 (September 1992): 1086–100. http://dx.doi.org/10.1130/0016-7606(1992)104<1086:msamho>2.3.co;2.

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11

Satarugsa, P. "Cenozoic tectonic evolution of the Ruby Mountains metamorphic core complex and adjacent valleys, northeastern Nevada." Rocky Mountain Geology 35, no. 2 (December 1, 2000): 205–30. http://dx.doi.org/10.2113/35.2.205.

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12

Wannamaker, Philip E., and William M. Doerner. "Crustal structure of the Ruby Mountains and southern Carlin Trend region, Nevada, from magnetotelluric data." Ore Geology Reviews 21, no. 3-4 (December 2002): 185–210. http://dx.doi.org/10.1016/s0169-1368(02)00089-6.

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13

Rickart, Eric A., Klaus G. Bienek, and Rebecca J. Rowe. "Impact of Livestock Grazing on Plant and Small Mammal Communities in the Ruby Mountains, Northeastern Nevada." Western North American Naturalist 73, no. 4 (December 2013): 505–15. http://dx.doi.org/10.3398/064.073.0403.

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14

BARNES, C. G. "Petrology and Geochemistry of the Late Eocene Harrison Pass Pluton, Ruby Mountains Core Complex, Northeastern Nevada." Journal of Petrology 42, no. 5 (May 1, 2001): 901–29. http://dx.doi.org/10.1093/petrology/42.5.901.

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15

Dokka, Roy K., Michael J. Mahaffie, and Arthur W. Snoke. "Thermochronologic evidence of major tectonic denudation associated with detachment faulting, Northern Ruby Mountains - East Humboldt Range, Nevada." Tectonics 5, no. 7 (December 1986): 995–1006. http://dx.doi.org/10.1029/tc005i007p00995.

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16

Zuza, Andrew V., Charles H. Thorman, Christopher D. Henry, Drew A. Levy, Seth Dee, Sean P. Long, Charles A. Sandberg, and Emmanuel Soignard. "Pulsed Mesozoic Deformation in the Cordilleran Hinterland and Evolution of the Nevadaplano: Insights from the Pequop Mountains, NE Nevada." Lithosphere 2020, no. 1 (August 25, 2020): 1–24. http://dx.doi.org/10.2113/2020/8850336.

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Abstract Mesozoic crustal shortening in the North American Cordillera’s hinterland was related to the construction of the Nevadaplano orogenic plateau. Petrologic and geochemical proxies in Cordilleran core complexes suggest substantial Late Cretaceous crustal thickening during plateau construction. In eastern Nevada, geobarometry from the Snake Range and Ruby Mountains-East Humboldt Range-Wood Hills-Pequop Mountains (REWP) core complexes suggests that the ~10–12 km thick Neoproterozoic-Triassic passive-margin sequence was buried to great depths (>30 km) during Mesozoic shortening and was later exhumed to the surface via high-magnitude Cenozoic extension. Deep regional burial is commonly reconciled with structural models involving cryptic thrust sheets, such as the hypothesized Windermere thrust in the REWP. We test the viability of deep thrust burial by examining the least-deformed part of the REWP in the Pequop Mountains. Observations include a compilation of new and published peak temperature estimates (n=60) spanning the Neoproterozoic-Triassic strata, documentation of critical field relationships that constrain deformation style and timing, and new 40Ar/39Ar ages. This evidence refutes models of deep regional thrust burial, including (1) recognition that most contractional structures in the Pequop Mountains formed in the Jurassic, not Cretaceous, and (2) peak temperature constraints and field relationships are inconsistent with deep burial. Jurassic deformation recorded here correlates with coeval structures spanning western Nevada to central Utah, which highlights that Middle-Late Jurassic shortening was significant in the Cordilleran hinterland. These observations challenge commonly held views for the Mesozoic-early Cenozoic evolution of the REWP and Cordilleran hinterland, including the timing of contractional strain, temporal evolution of plateau growth, and initial conditions for high-magnitude Cenozoic extension. The long-standing differences between peak-pressure estimates and field relationships in Nevadan core complexes may reflect tectonic overpressure.

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17

Dallmeyer, R. D., A. W. Snoke, and E. H. McKee. "The Mesozoic-Cenozoic tectonothermal evolution of the Ruby Mountains, East Humboldt Range, Nevada: A Cordilleran Metamorphic Core Complex." Tectonics 5, no. 6 (October 1986): 931–54. http://dx.doi.org/10.1029/tc005i006p00931.

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18

Hurlow, Hugh A., Arthur W. Snoke, and Kip V. Hodges. "Temperature and pressure of mylonitization in a Tertiary extensional shear zone, Ruby Mountains-East Humboldt Range, Nevada: Tectonic implications." Geology 19, no. 1 (1991): 82. http://dx.doi.org/10.1130/0091-7613(1991)019<0082:tapomi>2.3.co;2.

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19

Stoerzel, Andreas, and Scott B. Smithson. "Two-dimensional travel time inversion for the crustalPandSwave velocity structure of the Ruby Mountains metamorphic core complex, NE Nevada." Journal of Geophysical Research: Solid Earth 103, B9 (September 10, 1998): 21121–43. http://dx.doi.org/10.1029/98jb01494.

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20

Haines, Samuel H., and Ben A. van der Pluijm. "Dating the detachment fault system of the Ruby Mountains, Nevada: Significance for the kinematics of low-angle normal faults." Tectonics 29, no. 4 (August 2010): n/a. http://dx.doi.org/10.1029/2009tc002552.

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21

Hawman, Robert B., and Hishameldin O. Ahmed. "Shallow seismic reflection profiling over a Mylonitic Shear Zone, Ruby Mountains-East Humboldt Range Metamorphic Core Complex, NE Nevada." Geophysical Research Letters 22, no. 12 (June 15, 1995): 1545–48. http://dx.doi.org/10.1029/95gl01410.

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22

Zuza, Andrew V., Christopher D. Henry, Seth Dee, Charles H. Thorman, and Matthew T. Heizler. "Jurassic–Cenozoic tectonics of the Pequop Mountains, NE Nevada, in the North American Cordillera hinterland." Geosphere 17, no. 6 (October 27, 2021): 2078–122. http://dx.doi.org/10.1130/ges02307.1.

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Abstract The Ruby Mountains–East Humboldt Range–Wood Hills–Pequop Mountains (REWP) metamorphic core complex, northeast Nevada, exposes a record of Mesozoic contraction and Cenozoic extension in the hinterland of the North American Cordillera. The timing, magnitude, and style of crustal thickening and succeeding crustal thinning have long been debated. The Pequop Mountains, comprising Neoproterozoic through Triassic strata, are the least deformed part of this composite metamorphic core complex, compared to the migmatitic and mylonitized ranges to the west, and provide the clearest field relationships for the Mesozoic–Cenozoic tectonic evolution. New field, structural, geochronologic, and thermochronological observations based on 1:24,000-scale geologic mapping of the northern Pequop Mountains provide insights into the multi-stage tectonic history of the REWP. Polyphase cooling and reheating of the middle-upper crust was tracked over the range of <100 °C to 450 °C via novel 40Ar/39Ar multi-diffusion domain modeling of muscovite and K-feldspar and apatite fission-track dating. Important new observations and interpretations include: (1) crosscutting field relationships show that most of the contractional deformation in this region occurred just prior to, or during, the Middle-Late Jurassic Elko orogeny (ca. 170–157 Ma), with negligible Cretaceous shortening; (2) temperature-depth data rule out deep burial of Paleozoic stratigraphy, thus refuting models that incorporate large cryptic overthrust sheets; (3) Jurassic, Cretaceous, and Eocene intrusions and associated thermal pulses metamorphosed the lower Paleozoic–Proterozoic rocks, and various thermochronometers record conductive cooling near original stratigraphic depths; (4) east-draining paleovalleys with ∼1–1.5 km relief incised the region before ca. 41 Ma and were filled by 41–39.5 Ma volcanic rocks; and (5) low-angle normal faulting initiated after the Eocene, possibly as early as the late Oligocene, although basin-generating extension from high-angle normal faulting began in the middle Miocene. Observed Jurassic shortening is coeval with structures in the Luning-Fencemaker thrust belt to the west, and other strain documented across central-east Nevada and Utah, suggesting ∼100 km Middle-Late Jurassic shortening across the Sierra Nevada retroarc. This phase of deformation correlates with terrane accretion in the Sierran forearc, increased North American–Farallon convergence rates, and enhanced Jurassic Sierran arc magmatism. Although spatially variable, the Cordilleran hinterland and the high plateau that developed across it (i.e., the hypothesized Nevadaplano) involved a dynamic pulsed evolution with significant phases of both Middle-Late Jurassic and Late Cretaceous contractional deformation. Collapse long postdated all of this contraction. This complex geologic history set the stage for the Carlin-type gold deposit at Long Canyon, located along the eastern flank of the Pequop Mountains, and may provide important clues for future exploration.

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23

Cooper, Frances J., John P. Platt, and Whitney M. Behr. "Rheological transitions in the middle crust: insights from Cordilleran metamorphic core complexes." Solid Earth 8, no. 1 (February 21, 2017): 199–215. http://dx.doi.org/10.5194/se-8-199-2017.

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Abstract. High-strain mylonitic rocks in Cordilleran metamorphic core complexes reflect ductile deformation in the middle crust, but in many examples it is unclear how these mylonites relate to the brittle detachments that overlie them. Field observations, microstructural analyses, and thermobarometric data from the footwalls of three metamorphic core complexes in the Basin and Range Province, USA (the Whipple Mountains, California; the northern Snake Range, Nevada; and Ruby Mountains–East Humboldt Range, Nevada), suggest the presence of two distinct rheological transitions in the middle crust: (1) the brittle–ductile transition (BDT), which depends on thermal gradient and tectonic regime, and marks the switch from discrete brittle faulting and cataclasis to continuous, but still localized, ductile shear, and (2) the localized–distributed transition, or LDT, a deeper, dominantly temperature-dependent transition, which marks the switch from localized ductile shear to distributed ductile flow. In this model, brittle normal faults in the upper crust persist as ductile shear zones below the BDT in the middle crust, and sole into the subhorizontal LDT at greater depths.In metamorphic core complexes, the presence of these two distinct rheological transitions results in the development of two zones of ductile deformation: a relatively narrow zone of high-stress mylonite that is spatially and genetically related to the brittle detachment, underlain by a broader zone of high-strain, relatively low-stress rock that formed in the middle crust below the LDT, and in some cases before the detachment was initiated. The two zones show distinct microstructural assemblages, reflecting different conditions of temperature and stress during deformation, and contain superposed sequences of microstructures reflecting progressive exhumation, cooling, and strain localization. The LDT is not always exhumed, or it may be obscured by later deformation, but in the Whipple Mountains, it can be directly observed where high-strain mylonites captured from the middle crust depart from the brittle detachment along a mylonitic front.

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24

Vogler, D. R., and D. A. Charlet. "First Report of the White Pine Blister Rust Fungus (Cronartium ribicola) Infecting Whitebark Pine (Pinus albicaulis) and Ribes spp. in the Jarbidge Mountains of Northeastern Nevada." Plant Disease 88, no. 7 (July 2004): 772. http://dx.doi.org/10.1094/pdis.2004.88.7.772b.

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The Jarbidge Mountains are a remote and little-visited desert mountain range at the northern edge of the Great Basin in Elko County, NV, 110 km north of Elko and 115 km southwest of Twin Falls, ID. The forest is dominated by subalpine fir (Abies lasiocarpa) at lower elevations and whitebark pine (Pinus albicaulis) at higher elevations; limber pine (P. flexilis) occurs along streams in canyons at lower elevations (2). P. albicaulis and P. flexilis are hosts for the blister rust fungus, Cronartium ribicola. In the late 1990s, a survey across the Intermountain West reported no evidence of C. ribicola in the Jarbidge Mountains or elsewhere in the central Great Basin (3). However, unpublished observations by D. A. Charlet in 1988 and 2001 indicate that blister rust has been present in the Jarbidge Mountains for at least 16 years. In September 2002, D. R. Vogler visited the Jarbidge Mountains over a 2-week period, examining whitebark pines along the unpaved route through the Humboldt-Toiyabe National Forest connecting Highway 225 and Jarbidge, NV. Blister rust-infected whitebark were found in two locations: (i) Coon Creek Summit (2,575 m elevation), atop the divide between the Great Basin to the south and the Columbia Plateau to the north, and (ii) Bear Creek drainage (2,315 to 2,405 m elevation), 6.7 km northeast of Coon Creek Summit. At Coon Creek Summit, three whitebark pines ranging in diameter from 10 to 30 cm at breast height (dbh) were infected (evidenced by spindle-shaped branch swellings, aecia, and aeciospores), with the oldest infection occurring on wood produced in 1975. Assuming a mean needle retention of 10 years, the first pine infection likely occurred between 1975 and 1984. Ribes montigenum and an unknown Ribes sp. were common at Coon Creek Summit but were not infected. In the Bear Creek drainage north of the divide, 27 whitebark pines ranging in size from under 0.3 m high to 12 cm dbh were found infected, with the oldest infection on 1976 wood indicating an origin between 1976 and 1985. Most pines there, however, appeared to have been infected between 1994 and 1998. At Bear Creek, infection on Ribes spp. was common, with R. cereum the most frequently infected species. Voucher specimens of R. cereum (KPK-948 and KPK-949) are archived in the fungal herbarium at the Institute of Forest Genetics, Placerville, CA. On pine, fresh spermatia and aeciospores were abundant even though it was late in the season. Late sporulation has also been observed above 2,500 m on western white (P. monticola) and whitebark pine northeast of Lake Tahoe in Nevada (4). To our knowledge, our report marks the first recorded intrusion by C. ribicola into the north-central Great Basin. Recently, the first report of C. ribicola on Rocky Mountain bristlecone pine (P. aristata) was documented in southern Colorado (1). Now, Great Basin bristlecone (P. longaeva), which is restricted in Nevada to higher elevations in the eastern and southern parts of the state (2), may also be at risk; the northernmost occurrence of this last whitepine holdout from blister rust is in the Ruby Mountains, 135 km south of our findings in the Jarbidge Mountains. References: (1) J. T. Blodgett and K. F. Sullivan. Plant Dis. 88:311, 2004. (2) D. A. Charlet. Atlas of Nevada Conifers. University of Nevada Press, Reno, 1996. (3) J. P. Smith and J. T. Hoffman. Western North American Naturalist 60:165, 2000. (4) J. P. Smith et al. Plant Dis. 84:594. 2000.

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25

Hodges, K. V., A. W. Snoke, and H. A. Hurlow. "Thermal evolution of a portion of the Sevier Hinterland: The Northern Ruby Mountains-East Humboldt Range and Wood Hills, northeastern Nevada." Tectonics 11, no. 1 (February 1992): 154–64. http://dx.doi.org/10.1029/91tc01879.

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26

Hacker, Bradley R., An Yin, John M. Christie, and Arthur W. Snoke. "Differential stress, strain rate, and temperatures of mylonitization in the Ruby Mountains, Nevada: Implications for the rate and duration of uplift." Journal of Geophysical Research 95, B6 (1990): 8569. http://dx.doi.org/10.1029/jb095ib06p08569.

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27

MacCready, Tyler. "Misalignment of quartz c-axis fabrics and lineations due to oblique final strain increments in the Ruby Mountains core complex, Nevada." Journal of Structural Geology 18, no. 6 (June 1996): 765–76. http://dx.doi.org/10.1016/s0191-8141(96)80010-1.

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28

Wesnousky, Steven G., Richard W. Briggs, Marc W. Caffee, F. J. Ryerson, Robert C. Finkel, and Lewis A. Owen. "Terrestrial cosmogenic surface exposure dating of glacial and associated landforms in the Ruby Mountains-East Humboldt Range of central Nevada and along the northeastern flank of the Sierra Nevada." Geomorphology 268 (September 2016): 72–81. http://dx.doi.org/10.1016/j.geomorph.2016.04.027.

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29

Starratt, Scott W. "Diatom floras in lakes in the Ruby Mountains and East Humboldt Range, Nevada, USA: a tool for assessing high-elevation climatic variability." Nova Hedwigia, Beihefte 147 (October 4, 2018): 319–58. http://dx.doi.org/10.1127/nova-suppl/2018/024.

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30

Fricke, Henry C., Stephen M. Wickham, and James R. O'Neil. "Oxygen and hydrogen isotope evidence for meteoric water infiltration during mylonitization and uplift in the Ruby Mountains-East Humboldt Range core complex, Nevada." Contributions to Mineralogy and Petrology 111, no. 2 (1992): 203–21. http://dx.doi.org/10.1007/bf00348952.

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31

Wahl, D., S. Starratt, L. Anderson, J. Kusler, C. Fuller, J. Addison, and E. Wan. "Holocene environmental changes inferred from biological and sedimentological proxies in a high elevation Great Basin lake in the northern Ruby Mountains, Nevada, USA." Quaternary International 387 (November 2015): 87–98. http://dx.doi.org/10.1016/j.quaint.2015.03.026.

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32

Satarugsa, P., and R. A. Johnson. "Constraints on crustal composition beneath a metamorphic core complex: results from 3-component wide-angle seismic data along the eastern flank of the Ruby Mountains, Nevada." Tectonophysics 329, no. 1-4 (December 2000): 223–50. http://dx.doi.org/10.1016/s0040-1951(00)00197-9.

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33

Canada, Andrew S., Elizabeth J. Cassel, Daniel F. Stockli, M. Elliot Smith, Brian R. Jicha, and Brad S. Singer. "Accelerating exhumation in the Eocene North American Cordilleran hinterland: Implications from detrital zircon (U-Th)/(He-Pb) double dating." GSA Bulletin 132, no. 1-2 (May 16, 2019): 198–214. http://dx.doi.org/10.1130/b35160.1.

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AbstractBasins in orogenic hinterlands are directly coupled to crustal thickening and extension through landscape processes and preserve records of deformation that are unavailable in footwall rocks. Following prolonged late Mesozoic–early Cenozoic crustal thickening and plateau construction, the hinterland of the Sevier orogen of western North America underwent late Cenozoic extension and formation of metamorphic core complexes. While the North American Cordillera is one of Earth’s best-studied orogens, estimates for the spatial and temporal patterns of initial extensional faulting differ greatly and thus limit understanding of potential drivers for deformation. We employed (U-Th)/(He-Pb) double dating of detrital zircon and (U-Th)/He thermochronology of detrital apatite from precisely dated Paleogene terrestrial strata to quantify the timing and magnitude of exhumation and explore the linkages between tectonic unroofing and basin evolution in northeastern Nevada. We determined sediment provenance and lag time evolution (i.e., the time between cooling and deposition, which is a measure of upper-crustal exhumation) during an 8 m.y. time span of deposition within the Eocene Elko Basin. Fluvial strata deposited between 49 and 45 Ma yielded Precambrian (U-Th)/He zircon cooling ages (ZHe) with 105–740 m.y. lag times dominated by unreset detrital ages, suggesting limited exhumation and Proterozoic through early Eocene sediment burial (<4–6 km) across the region. Minimum nonvolcanic detrital ZHe lag times decreased to <100 m.y. in 45–43 Ma strata and to <10 m.y. in 43–41 Ma strata, illustrating progressive and rapid hinterland unroofing in Eocene time. Detrital apatite (U-Th)/He ages present in ca. 44 and 39 Ma strata record Eocene cooling ages with 1–20 m.y. lag times. These data reflect acceleration of basement exhumation rates by >1 km/m.y., indicative of rapid, large-magnitude extensional faulting and metamorphic core complex formation. Contemporaneous with this acceleration of hinterland exhumation, syntectonic freshwater lakes developed in the hanging wall of the Ruby Mountains–East Humboldt Range metamorphic core complex at ca. 43 Ma. Volcanism driven by Farallon slab removal migrated southward across northeastern Nevada, resulting in voluminous rhyolitic eruptions at 41.5 and 40.1 Ma, and marking the abrupt end of fluvial and lacustrine deposition across much of the Elko Basin. Thermal and rheologic weakening of the lithosphere and/or partial slab removal likely initiated extensional deformation, rapidly unroofing deeper crustal levels. We attribute the observed acceleration in exhumation, expansion of sedimentary basins, and migrating volcanism across the middle Eocene to record the thermal and isostatic effects of Farallon slab rollback and subsequent removal of the lowermost mantle lithosphere.

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34

Klingler, Kelly B., Joshua P. Jahner, Thomas L. Parchman, Chris Ray, and Mary M. Peacock. "Genomic variation in the American pika: signatures of geographic isolation and implications for conservation." BMC Ecology and Evolution 21, no. 1 (January 21, 2021). http://dx.doi.org/10.1186/s12862-020-01739-9.

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Abstract Background Distributional responses by alpine taxa to repeated, glacial-interglacial cycles throughout the last two million years have significantly influenced the spatial genetic structure of populations. These effects have been exacerbated for the American pika (Ochotona princeps), a small alpine lagomorph constrained by thermal sensitivity and a limited dispersal capacity. As a species of conservation concern, long-term lack of gene flow has important consequences for landscape genetic structure and levels of diversity within populations. Here, we use reduced representation sequencing (ddRADseq) to provide a genome-wide perspective on patterns of genetic variation across pika populations representing distinct subspecies. To investigate how landscape and environmental features shape genetic variation, we collected genetic samples from distinct geographic regions as well as across finer spatial scales in two geographically proximate mountain ranges of eastern Nevada. Results Our genome-wide analyses corroborate range-wide, mitochondrial subspecific designations and reveal pronounced fine-scale population structure between the Ruby Mountains and East Humboldt Range of eastern Nevada. Populations in Nevada were characterized by low genetic diversity (π = 0.0006–0.0009; θW = 0.0005–0.0007) relative to populations in California (π = 0.0014–0.0019; θW = 0.0011–0.0017) and the Rocky Mountains (π = 0.0025–0.0027; θW = 0.0021–0.0024), indicating substantial genetic drift in these isolated populations. Tajima’s D was positive for all sites (D = 0.240–0.811), consistent with recent contraction in population sizes range-wide. Conclusions Substantial influences of geography, elevation and climate variables on genetic differentiation were also detected and may interact with the regional effects of anthropogenic climate change to force the loss of unique genetic lineages through continued population extirpations in the Great Basin and Sierra Nevada.

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