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31	Prehistoric Timberline Adaptations in the Eastern Uinta Mountains, Utah Knoll, Michelle 12 September 2003 (has links) (PDF) Excavations at a high altitude archaeological site (3350 m) in the eastern Uinta Mountains, Utah, uncovered at least three ephemeral brush structures. These temporary timberline dwellings are the highest structures excavated in Utah to date. The periods of occupation range from the early Fremont period to the post-contact era. It is believed that the Fremont occupations are logistical in nature, possibly representing male hunting parties. Logistical camps imply a departure from, and return to, a residential camp. Ethnographic studies show that most residential camps are located within proximity to culinary plants to facilitate collection by women. In the Uinta Mountains, residential camps were most likely located at mid-elevations for the procurement of Chenopodium seeds. In addition to the benefits women received by being close to an important economic resource, mid-elevation bases meant that logistical male hunting parties could access the upper-most elevations more efficiently. A maximum transport distance model was tested for appropriateness at high altitudes. Maximum transport distance models measure levels of efficiency to and from a residential base (or, more correctly, to a point of consumption). They are mathematical models built on measures of caloric gain and expenditure. It is argued that efficiency models that focus on male economic tasks, typically expected at timberline sites, must also consider where the residential base will be located based on women's subsistence economies. In other words, in order to operate above a caloric loss the maximum return trip distance for a male hunter laden with a resource must reach the residential base. However, as stated earlier, the location of the residential base should be located where women could collect most efficiently, not at the male's maximum distance. Thus, the male logistical zone (from timberline to the residence) and the female residential zone must overlap, or the maximum transport model cannot be supported. In this case, other currencies, such as prestige and fatty meat, could have propelled an individual to travel farther that energy-based transport models allow. archaeology timberline Uinta Mountains Utah maximum transport distance models Deadman Lake Fremont period adaptations Anthropology
32	Pre-Historic Landslides on the Southeast Flank of the Uinta Mountains, Utah: Character and Causes of Slope Failure Bradfield, Todd D. 16 March 2007 (has links) (PDF) More than 100 landslides have been mapped along the southeast flank of the Uinta Mountains. Large landslide deposits are up to 4.6 kilometers long and have an area of approximately 5-9 km². Landslide types include multiple and successive rock slumps, debris slumps and debris flows. Most landslides have a main head scarp in the Bishop Conglomerate and the large landslides have many minor scarps. Multiple slump blocks are manifest by repeated transverse ridges and trenches in the head area of some landslides. Most body and toe areas are deeply incised by gully erosion (up to 91 meters deep) and drainages are well developed with little ponding. Detailed mapping of the large landslides shows that the deposits are an accumulation of successive slope failures that have continually eroded the landscape over time. Many landslides in the area appear to be inactive and dormant but slopes may continue to fail particularly if landslides are disturbed. A Geographic Information System (GIS) was used to analyse slope failing factors and the main factor that seems to have contributed to slope failure is the presence of abundant shale-rich, weak bedrock capped with the thick and fairly resistant Bishop Conglomerate. Slopes are further destabilized as water percolates down through the porous Bishop Conglomerate. Eventually the water meets underlying shale-rich bedrock where it is channelled near this contact until it emerges as springs. This groundwater flow likely reduces shear strength of the shale-rich substrate and of some of the finer grained layers in the Bishop Conglomerate. Other important slope failure factors include the removal of easily erodable Mesozoic shales from beneath the more-resistant Bishop Conglomerate, headward gully erosion, bedrock dip and slope aspect. landslide GIS uinta mountain bishop conglomerate slope failing analysis slump Geology
33	STRATIGRAPHY AND PALYNOLOGY OF THE ALBIAN-CENOMANIAN DAKOTA FORMATION AND MOWRY SHALE, UINTA BASIN, UTAH AND COLORADO Pierson, Justin Scott 01 December 2009 (has links) No description available. Geology Stratigraphy Palynology Cretaceous Dakota Formation Mowry Shale Uinta Basin Utah Colorado
34	Mapping and Kinematic Structural Analysis of the Deep Creek Fault Zone, South Flank of the Uinta Mountains, Near Vernal, Utah Haddox, David A. 11 May 2005 (has links) (PDF) The geology along the southern flank of the Uinta Mountains, located north of Vernal, Utah, has been mapped at the 7.5' scale within two quadrangles: the Dry Fork and Steinaker Reservoir Quadrangles. Ambiguities dealing with stratigraphy, structural geology, and geohazards are currently being addressed as a result of this and other mapping projects in the vicinity. The geologic units in the area range in age from Mississippian to Late Cretaceous and include Uinta-sourced Tertiary units. Brief unit descriptions are provided for each of the units exposed in the map area. The main structural influence on the rocks within the area is that of the Uinta Uplift and its southern bounding fault, the Uinta Basin Boundary thrust. Locally, the Deep Creek fault zone overprints and dissects the southernmost flank of the broad Uinta Anticline. Other smaller structurally complex areas and folds exist east of the Deep Creek fault zone. The Deep Creek fault zone is made up of a series of NW-SE trending faults, likely related to the South Flank fault zone. Many authors have inferred dip-slip movement along the South Flank fault zone, but have not supported these claims using kinematic data. Detailed mapping and kinematic data collected within the study area has produced a better understanding of the deformation history along the fault zones in question. The faults within the Deep Creek fault zone have steep, linear traces upon which both vertical dip-slip and very nearly strike-slip (left-lateral oblique-slip, mainly) movement has occurred. The faults of the Deep Creek fault zone are likely Paleocene in age. The data suggest a bimodal history of deformation which the principal stress field does not seem to be influenced by typical east-northeast-west-southwest Laramide orogenic far-field stresses. The creation and early history of these faults may have been due to localized stress fields related to activity of the underlying Uinta Basin Boundary thrust, or a later period of uplift, a possible accommodation zone between the western and eastern domes of the Uinta Mountain Range, a transfer zone between the Uinta Basin Boundary thrust and the Asphalt Ridge fault, or a combination of these. Deep Creek fault zone South Flank fault zone Uinta Mountains Vernal northeastern Utah Dry Fork Steinaker Reservoir Geology
35	SEQUENCE STRATIGRAPHY OF THE CURTIS, SUMMERVILLE AND STUMP FORMATIONS, UTAH AND NORTHWEST COLORADO Wilcox, William Thomas 24 April 2007 (has links) No description available. Geology Sequence Stratigraphy Utah Curtis Formation Summerville Formation Stump Formation Uinta Mountains San Rafael Swell Oxfordian Palynology Ammonites
36	Piecing Together the Triassic/Jurassic Stratigraphy Along the South Flank of the Uinta Mountains, Northeast Utah: A Stratigraphic Analysis of the Bell Springs Member of the Nugget Sandstone Jensen, Paul H., Jr. 04 August 2005 (has links) (PDF) Nomenclature for the Upper Triassic and Lower Jurassic strata along the south flank of the Uinta Mountains has been somewhat confusing because of the position of the study area between southern Wyoming, where one set of names is used, and central/southern Utah where a different set of formation names is used. The Nugget Sandstone or Glen Canyon Sandstone of the eastern Uinta Mountains overlies the Upper Triassic Popo Agie or Chinle Formation. The nature of the contact between these two formations is unclear both in stratigraphic location and conformability. The Chinle Formation consists, in ascending order, of the Gartra Member, the purple unit, the ocher unit, and the upper red unit. The overlying Nugget Sandstone consists of two members, the lower Bell Springs Member and the overlying unnamed cross-bedded member, typically believed to be Navajo Sandstone equivalent. These two units of the Nugget Sandstone are thought to represent the Glen Canyon Group of the Colorado Plateau, although no obvious Wingate or Kayenta Formation equivalents have been recognized. The Bell Springs Member contains abundant fine-grained, ripple-laminated sandstones, red and green mudstones, occasional mudcracks and salt casts, evidence of burrowing and exposure, and some medium- to coarse-grained sandstones with small-scale (30-40 cm high) cross-beds. This member was deposited in a marine tidal flat environment, quite different from the mainly eolian environment of the rest of the Nugget Sandstone. The Bell Springs Member appears to be entirely Upper Triassic, based upon dinosaur tracks, while the upper windblown unit's age is unknown, but probably straddles the Triassic-Jurassic boundary. During mapping in the Donkey Flat, Steinaker Reservoir, Dry Fork, and Lake Mountain quadrangles, the Bell Springs Member of the Nugget Sandstone was mapped as a separate unit. geology Triassic Jurassic stratigraphy south flank Uinta Mountains Northeast Utah stratigraphic analysis Bell Springs Member Nugget Sandstone Vernal Donkey Flat Red Fleet Geology
37	Basinward Trends in Fluvial Architecture, Connectivity, and Reservoir Characterization of the Trail Member, Ericson Sandstone, Mesaverde Group in Wyoming, Utah, and Colorado, USA Jolley, Chelsea Anne 01 June 2019 (has links) The Late Cretaceous Trail Member of the Ericson Sandstone represents a regionally extensive fluvial system that transported sediments from the Sevier fold and thrust belt and Uinta Mountain uplift to the Western Interior Seaway. The Trail Member is a petroleum reservoir target that has unpredictable production rates due to the unknown behavior and connectivity of channel sandstones. The abundant outcrop, wellbore, and core data available allows for a comprehensive analysis of how the fluvial architecture, connectivity, and reservoir quality change along 65 km of depositional dip. Observations made at Flaming Gorge and Clay Basin (most landward field locations) suggest a highly mobile fluvial system that was influenced by both autogenic channel clustering and allogenic forcing. Evidence is seen for movement along the Sevier fold and thrust belt and early Laramide uplift of the Uinta Mountains. Specifically, three zones identify temporal tectonic changes throughout deposition of the Trail Member. The Upper and Lower Trail zones represent times of low accommodation as the fluvial system must avulse and move laterally to find available space. The Middle Trail zone represents a higher accommodation setting with internal autogenic channel clustering. This shows that on a finer timescale, autogenic processes control sediment distribution, while on a longer timescale, external drivers, specifically tectonics, control the distribution of sediment in the Trail fluvial system. Significant changes were observed within the Trail Member towards the basin. At Northern Colorado, lenticular, fluvial-dominated sands are still common, preserved organic and woody material, mud cracks, and increased bioturbation are observed that are not present elsewhere. The sandstone channels are slightly wider, have more common occurrences of low flow-regime sedimentary structures such as ripples and mud cracks, and appear to be more individually isolated with thin fine-grained material surrounding the channels. On a larger scale, photogrammetric analysis shows a rapid lateral change (0.3 km) from a sand-rich, channel-dominated expression to a mud-rich, channel-poor character. These observations suggest a lower energy fluvial system focused within a possible incised valley showing that the fluvial system is being influenced primarily by eustatic forces, rather than tectonics. Subsurface data from twelve wells located north of the Northern Colorado locality show a rapid (15 km) increase in thickness (97 m to 182 m) and decrease in net-to-gross (89.3% to 65.3%). Early subsidence of the Washakie sub-basin just east of the wells could account for the rapid increase in accommodation. Another possible explanation for the rapid thickness increase to the northeast could be the presence of an incised valley. These possibilities show the complexity of the environment within which the Trail Member fluvial system deposited sediments. Trail Member porosity and permeability net-to-gross fluvial architecture Sevier fold and thrust belt Uinta Mountain uplift reservoir photogrammetry facies Geology Physical Sciences and Mathematics
38	Geology of the Phil Pico Mountain Quadrangle, Daggett County, Utah, and Sweetwater County, Wyoming Anderson, Alvin D. 25 April 2008 (has links) (PDF) Geologic mapping in the Phil Pico Mountain quadrangle and analysis of the Carter Oil Company Carson Peak Unit 1 well have provided additional constraints on the erosional and uplift history of this section of the north flank of the Uinta Mountains. Phil Pico Mountain is largely composed of the conglomeratic facies of the early Eocene Wasatch and middle to late Eocene Bridger Formations. These formations are separated by the Henrys Fork fault which has thrust Wasatch Formation next to Bridger Formation. The Wasatch Formation is clearly synorogenic and contains an unroofing succession from the adjacent Uinta Mountains. On Phil Pico Mountain, the Wasatch Formation contains clasts eroded sequentially from the Permian Park City Formation, Permian Pennsylvanian Weber Sandstone, Pennsylvanian Morgan Formation, and the Pennsylvanian Round Valley and Mississippian Madison Limestones. Renewed uplift in the middle and late Eocene led to the erosion of Wasatch Formation and its redeposition as Bridger Formation on the down-thrown footwall of the Henrys Fork fault. Field observations and analysis of the cuttings and lithology log from Carson Peak Unit 1 well suggest that initial uplift along the Henrys Fork Fault occurred in the late early or early middle Eocene with the most active periods of uplift in the middle and late Eocene (Figure 8, Figure 24, Appendix 1). The approximate post-Paleocene throw of the Henrys Fork fault at Phil Pico Mountain is 2070 m (6800 ft). The Carson Peak Unit 1 well also reveals that just north of the Henrys Fork fault at Phil Pico Mountain the Bridger Formation (middle to late Eocene) is 520 m (1710 ft) thick; an additional 460 m (1500 ft) of Bridger Formation lies above the well on Phil Pico Mountain. Beneath the Bridger Formation are 400 m (1180 ft) of Green River Formation (early to middle Eocene), 1520 m (5010 ft) of Wasatch Formation (early Eocene), and 850 m (2800 ft) of the Fort Union Formation (Paleocene). Stratigraphic data from three sections located east to west across the Phil Pico Mountain quadrangle show that the Protero-zoic Red Pine Shale has substantially more sandstone and less shale in the eastern section of the quadrangle. Field observations suggest that the Red Pine Shale undergoes a facies change across the quadrangle. However, due to the lack of continuous stratigraphic exposures, the cause of this change is not known. Eocene Red Pine Shale Uinta Mountains Bridger Formation Wasatch Formation Henrys Fork Fault Uplift uplift history anticline syncline Laramide Green River Formation Bishop Conglomerate inverted cobble stratigraphy unroofing unroofing sequence conglomerate Phil Pico Mountain Flaming Gorge Utah Wyoming Paleocene clast erosional history north flank facies change strike-slip fault Madison Limestone Weber Sandstone Vr VrTwo VrOne geologic mapping geology glacial deposits Smiths Fork Uinta thrust cuttings lithology log erosion Carson Peak well geologic map cross-section stratigaphy stratigraphic column unit descriptions tectonic history Tertiary depositional deposition Proterozoic Precambrian Geology

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