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glacial geologic map of the uinta mountains area, utah and wyoming

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Box 146100, Salt Lake City, UT 84114-6100 (801) 537-3300 geology.utah.gov This map was created from the Geographic Information System (GIS) data that accompanies this publication. Ql Qaf Qgr Qmt Qms Qal Qgu Qgau Qgb Qgab Qgs Qgo Qgas Qgao Qg/rx Qg/rx Qg/rx ? ? ? ? ? ? ? ? ? ? ? 11,500 yr 126,000 yr 781,000 yr Holocene Late Pleistocene Middle Pleistocene Early Pleistocene QUATERNARY Alluvial Deposits Lacustrine Deposits Glacial Deposits Mass-movement Deposits ? Qgu Qgau Periglacial Deposits ? ? ? Wyoming Utah Utah Wyoming Provo Vernal Ogden Evanston Duchesne Dutch John Kings Peak Salt Lake City Firehole Canyon WYOMING UTAH UTAH WYOMING UINTA- WASATCH- CACHE NATIONAL FOREST ASHLEY NATIONAL FOREST ASHLEY NATIONAL FOREST UINTA- WASATCH- CACHE NATIONAL FOREST Mirror Lake H i g h w a y ! ( 35 ! ( 150 ! ( 35 WASATCH CO DUCHESNE CO DUCHESNE CO UINTAH CO DAGGETT CO UINTAH CO SUMMIT CO DAGGETT CO SUMMIT CO DUCHESNE CO SUMMIT CO WASATCH CO Lake Fork River Yellowstone River Rock Creek West Fork Duchesne River North Fork Duchesne River Soapstone Creek North Fork Provo River Weber River West Fork Bear River Bear River East Fork Bear River Blacks Fork Smiths Fork Henrys Fork West Fork Beaver Creek Middle Fork Beaver Creek Thompson Creek Burnt Fork Middle Fork Sheep Creek South Fork Sheep Creek West Fork Carter Creek East Fork Carter Creek North Fork Ashley Creek South Fork Ashley Creek Whiterocks River Dry Fork Uinta River Crow Canyon Beaver Creek Western Uintas Ice Field 111° 110° 41° 40° 10 0 10 5 KILOMETERS 10 0 10 5 MILES SCALE 1:500,000 Qal Qaf Qms Qmt Qgr Ql Qg/rx Qgs Qgas Qgb Qgab Qgu Qgau Qgo Qgao rx SYNOPSIS OF GLACIAL HISTORY Over the past roughly two million years of Earth history, known as the Quaternary Period, numerous climatic cycles led to the advance and retreat of glaciers worldwide. During each period of ice advance, or glaciation, global ice extent increased two- to three-fold and sea level fell more than 100 m as ocean water was stored as glacier ice on the continents. At high latitudes, ice sheets formed and expanded in North America and Eurasia to extents similar to or larger than that of the modern Antarctic ice sheet. Elsewhere, mountain glaciers advanced far down valleys, even in ranges currently devoid of glaciers. In the Uinta Mountains, a spectacular glacial landscape attests to the cumulative impact of these multiple glaciations during which erosion by ice produced numerous cirques, high basins, and U-shaped valleys, and enhanced the topographic relief between valleys and the high ridgelines. Some of the most impressive cirques in the range include the large basin holding Red Castle Lake at the head of the East Fork Smiths Fork, and the basin containing Walk-Up Lake at the head of the East Fork Whiterocks River. In places where cirques coalesced, broad basins formed, such as Painter Basin, Brown Duck Basin, and the Grandaddy Lake area. The U-shaped cross section of the Provo, Duchesne, and Bear River valleys can be seen from parts of the Mirror Lake Highway. Material eroded from the core of the Uinta Mountains was deposited by ice and glacial meltwater at lower elevations. Sediment deposited directly by glacier ice is called till, which can form ridges known as moraines that outline the lower margins of former glaciers. Some of the best preserved and most visible moraines in the Uinta Mountains are the sequence of sage- and Ponderosa pine-covered ridges impounding the Twin Pots Reservoir south of Moon Lake. Sediment deposited by glacial meltwater, known as outwash, is found downstream from moraines and forms terraces above the modern rivers. Much of the Mirror Lake Highway south of Evanston, Wyoming, follows outwash of the Bear River. Lone Tree, Wyoming, is situated on a broad outwash surface deposited by meltwater from the Henrys Fork, West Fork Beaver Creek, and Middle Fork Beaver Creek glaciers. Although geologic records from the oceans and ice sheets reveal that dozens of glaciations have occurred during the Quaternary Period, terrestrial records of this time interval are dominated by the most recent glaciations, which obliterated or buried evidence of the older events. On this map, the “Qgo” and “Qgao” units mark fragmentary evidence of older glaciations in the Uinta Mountains, such as the extensive lateral moraines and outwash east of the Yellowstone River. Although the ages of these older glaciations are not known in the Uinta Mountains, similar deposits in the Wind River Range of Wyoming are older than a 660,000-year-old volcanic ash (Chadwick and others, 1997). Deposits of the second-to-last glaciation, the Blacks Fork Glaciation, are more extensive. Prominent landforms of this event include lateral moraines along the Blacks Fork River north of Meeks Cabin Reservoir and along the east side of the Yellowstone River. Although the age of this event has not been directly determined in the Uinta Mountains, recent work on correlative deposits of the Bull Lake Glaciation in northwestern Wyoming suggests that it occurred between 160,000 to 130,000 years ago, or possibly between 120,000 to 95,000 years ago (Chadwick and others, 1997; Sharp and others, 2003; Licciardi and Pierce, 2008). The last glaciation in the Uinta Mountains is named the Smiths Fork Glaciation after the prominent terminal moraine in the East Fork Smiths Fork valley (Bradley, 1936). Deposits of this event are widespread and the timing of the Smiths Fork Glaciation has been directly determined from geologic ages of moraines in several valleys. These results indicate that ice advance began about 32,000 years ago, culminated 25,000 years ago, and glaciers began retreating from their terminal moraines by 16,000 years ago. These results also indicate that the Smiths Fork Glaciation occurred at essentially the same time as the Pinedale Glaciation elsewhere in the Rocky Mountains (Laabs and others, 2007, 2009). The Uinta Mountains were largely ice free by 14,000 years ago, although moraines in some cirques and high basins may represent glacial activity near the Pleistocene-Holocene transition. The highest moraines in the most favorably oriented cirques may also reflect more recent small-scale glacier activity. Although these moraines have not been directly dated, similar deposits of this “Neoglacial” interval in the Wind River Range have been dated to the past 5,000 years (Dahms, 2002). Many of the rock glaciers in the Uinta Mountains also likely formed or were reactivated during this time interval. DESCRIPTION OF THE ICE EXTENTS INSET MAP This inset map displays reconstructed ice extents for the Smiths Fork Glaciation (ca. 32,000 to 14,000 years ago) in the Uinta Mountains, determined through field observations coupled with interpretation of maps and aerial photographs. Upper ice limits were defined by inflection points in cirque headwalls, and trimlines. Lower ice limits were identified primarily by moraines, and by heads of outwash and ice-marginal channels. The western part of the Uinta Mountains was occupied by numerous small cirque and valley glaciers, along with the relatively broad Western Uintas Ice Field (Refsnider and others, 2007). This ice field inundated the crest of the range (except for the highest peaks) and drained into the Bear River, Weber River, Beaver Creek, North Fork Provo River, North Fork Duchesne, and Rock Creek valleys. The largest discrete valley glaciers developed in the central part of the Uinta Mountains where they flowed south and extended beyond the mountain front. Particularly large glaciers in the Lake Fork, Yellowstone, and Uinta River valleys were fed by broad, but confined, ice fields. In contrast, on the north slope of the Uinta Mountains ice advanced from numerous north-draining cirques to form long, narrow, valley glaciers. Glaciers in the Blacks Fork, Smiths Fork, and Henrys Fork valleys extended beyond the range front. In the West and Middle Fork Beaver Creeks, Thompson Creek, and Burnt Fork valleys, glaciers terminated at, or just south of, the range-bounding hogback. Glaciers in the Sheep Creek and Carter Creek valleys formed piedmont lobes on the north flank, south of the hogback. The smallest valley glaciers were found in the eastern part of the Uinta Mountains, where ice was entirely confined to valleys. The formation of few relatively large glaciers in southern valleys compared to several smaller glaciers in northern valleys is likely related to bedrock structure. Atwood (1909) suggested that gently-dipping bedrock on the south flank allowed Pleistocene glaciers to erode laterally more efficiently than glaciers on the north flank, leading to the formation of broad valleys at the heads of the Rock Creek, Lake Fork, Yellowstone, and Uinta River valleys. The floors of these valleys are above the estimated Smiths Fork-age equilibrium-line altitude (~3000 to 3100 m asl) for the central part of the range (Laabs and Carson, 2005), adding support for the notion that these large glaciers were sustained by broad accumulation areas. Alternatively, the formation of relatively large glaciers in south-central valleys may be due to climatic differences. Laabs and others (2007) proposed that regional southwest-to-northeast circulation during the Smiths Fork Glaciation may have delivered moisture-laden air masses to the southern part of the range, producing an orographic precipitation shadow over the northern valleys. There is also evidence for a longitudinal precipitation gradient running parallel to the range axis. As noted by Munroe and others (2006), glaciers in the western part of the Uinta Mountains extended to lower elevations and had equilibrium-line altitudes as low as 2600 m, which is ~600 m lower than glaciers farther east (~3200 m asl). This pattern reflects a tremendous enhancement of the modern asymmetric precipitation pattern in the Uinta Mountains, likely driven by the presence of pluvial Lake Bonneville, which was located within 60 km of the western Uinta Mountains and may have amplified precipitation in areas downwind. DESCRIPTION OF MAP UNITS Alluvium (Holocene) – Unconsolidated deposits of moderately to well-sorted and stratified clastic sediments, including gravel, sand, silt, and clay, formed by deposition in moving water. Stratigraphy consists of well-rounded clasts usually mantled by thin (< 1 m) finer-grained overbank deposits. The modern floodplain is inset within both glacial till and outwash deposits and wet and dry meadows are abundant. The present location and condition of the river or stream channel reflect the influence of postglacial disturbances including mass movements, Neoglacial activity, and human perturbations, including diversions and logging. Thickness is typically less than 10 m. Although alluvium is ubiquitous along modern streams, only the broadest and most continuous areas of alluvium are shown on the map. Alluvial-Fan Deposits (Holocene) – Unconsolidated, poorly to moderately sorted boulder-gravel, sand, silt, and clay. The lithology and grain size of the material comprising the fans reflects the rocks in the fan source area. For example, clay and silt derived from the Red Pine Shale dominate the large fan near the East Fork Blacks Fork Guard Station (section 23, T. 2 N., R. 12 E., Salt Lake Base Line and Meridian). Coarser boulders and gravel from the Bishop Conglomerate and Quaternary glacial deposits comprise the fan west of Meeks Cabin Reservoir in the Blacks Fork drainage (section 21, T. 3 N., R. 12 E., Salt Lake Base Line and Meridian). The alluvial fan below Dry Canyon in the Lake Fork drainage (section 24, T. 2 N., R. 6 W., Uinta Base Line and Meridian) is composed of coarse-grained sand and cobbles of Uinta Mountain Group quartzite derived from the Duchesne River Formation. Fans with a radial pattern of surface drainage extend outward from the base of a steep channel or chute cut through a lateral moraine or down a valley wall. Fans with hummocky surface topography owing to deposition primarily by mass wasting rather than alluvial activity are common below chutes, whereas fans with smooth surfaces are common below steep fluvial channels. Fan formation occurred through a combination of post-glacial fluvial and colluvial processes. Alluvial fans were mapped separately from cones of coarse, blocky debris produced by rockfall, which were mapped with talus (Qmt) and slides, slumps, and flows (Qms). Fan formation is apparently an episodic process linked to climatic factors including rate of snowmelt and rainfall. A single entrenched stream, reflecting relative stability, occupies many modern fans. However, bars and shallow channels visible on unvegetated fans (e.g., west of Meeks Cabin Reservoir) are evidence of past floods across the fan surface. Disturbances linked to fan progradation include the damming of the Stillwater Fork Bear River to produce Christmas Meadows (section 15, T. 1 N., R. 10 E., Salt Lake Base Line and Meridian), and impoundment of the Lake Fork River to form the pre-dam Moon Lake (section 18, T. 2 N., R. 5 W., Uinta Base Line and Meridian). Variable thickness from 1 to more than 10 m. Lacustrine Deposits (Holocene) – Unconsolidated lacustrine sediments, including laminated fine sand, silt and clay, and fine colluvium. Buried organic layers are also common. This deposit is commonly found in formerly closed depressions dammed by end moraines, till ridges, hummocks, and mass-wasting deposits. These basins are now marked by wet meadows and/or small lakes. Along major rivers, the landforms associated with this deposit are commonly distinguished by an abrupt change in channel sinuosity. Only the larger deposits are mapped; in areas of hummocky moraine or stagnant ice topography smaller versions of this deposit are ubiquitous. Christmas Meadows in the Stillwater Fork is a drained lake basin where water was temporarily impounded behind a set of alluvial fans. The large meadow below the ford on the West Fork Blacks Fork is impounded behind a recessional moraine complex. In the Middle Fork Blacks Fork a wet meadow marks the extent of a drained lake basin that was impounded behind slump deposits derived from the western valley wall. Cow Park and Little Meadow above Fish Creek are other examples of these deposits. Thickness is generally unknown, but may locally exceed 10 m. Slides, Slumps, and Flows (Holocene and Pleistocene [?]) – Unconsolidated, poorly sorted deposits of locally derived material that has moved down slope through landsliding, slumping, and flowing. Individual headscarps and rotated blocks can often be identified, and sag ponds are locally present where blocks are back-rotated (e.g., west side of Middle Fork Blacks Fork). Small mudflows and debris flows are common at the base of the scarps. The majority of slumps are located along the oversteepened sides of glaciated valleys where they are obviously post-glacial features. The mapped slumps and landslides on the north slope typically involve the Tertiary Wasatch Formation and overlying Bishop Conglomerate. Pleistocene glacial deposits are also incorporated where slumps occur along glaciated valley sides. Across the south slope, landslides are common along the bedrock contact between the Mississippian Doughnut (shale) and Humbug (limestone and sandstone) Formations. In some places, tributary valleys may have been dammed by lateral moraines and were subsequently filled by lakes. Failure of lateral moraine-dammed lakes may have instigated landslides in Lake Fork and Yellowstone canyons. Thickness is variable, but may exceed 100 m. Talus Deposits (Holocene and Pleistocene [?]) – Unconsolidated, poorly sorted deposits of angular boulders located at the base of cirque headwalls and along glacial valley sides. Blocks are detached from bedrock outcrops by freeze-thaw cycles, heavy rain, and snow avalanching. The surfaces of talus deposits are extremely coarse with fines having been removed by nival meltwater. Accumulations of fine colluvium are common down slope from many talus features, especially in settings below cliffs containing a large component of shale. Small, vegetated ridges of fine-grained material are present at the toe of many talus slopes, suggesting that the talus may be slowly moving outward from the source area. As mapped, talus deposits include broad sheet-like slopes, discrete avalanche cones, and series of coalesced cones, protalus ramparts, slushflow levee/channel complexes, small lobate rock glaciers, and small end moraines. In glaciated valleys, talus is post-glacial and presumably accumulated during more severe periglacial conditions in the latest Pleistocene. Some of the features may have been reactivated during the late Holocene Neoglacial period. Some talus deposits are active today, as evidenced by observed rock fall and fresh, lichen-free rocks. Thickness is generally unknown, but likely 1 to 50 m. Rock Glacier Deposits (Holocene and Pleistocene [?]) – Unconsolidated, poorly sorted deposits of angular boulders having a characteristic surface morphology owing to flow through deformation of interstitial ice. Fines are more common in these features than in talus, perhaps due to comminution of rock during movement or accumulation of eolian sediment. Fines may also be derived from shale layers exposed in the valley walls above the rock glacier, and may decrease the permeability of the talus sufficiently to allow formation of interstitial ice leading to rock glacier genesis. In plan view, rock glaciers take the form of lobate bulges extending outward from more uniform talus slopes, and of tongue-like masses occupying the floor of high-altitude cirque basins. Transverse ridges and furrows are common on rock glacier surfaces, indicating collapse of underlying zones of increased ice content during melt-out. Unstable, lichen-free, steep frontal slopes, and other features indicative of contemporary activity including surface meltwater ponds, are present on many of these features. Other rock glaciers, including most of those located along valley sides, appear to be stabilized, with gentler frontal slopes and greater lichen cover. Because of their locations within the glaciated valleys, all mapped rock glaciers are post-glacial in age. The exact timing of their formation is unknown, although it is likely that many of them formed in the latest Pleistocene and were reactivated during the Neoglaciation. Several rock glaciers in the study area, including the large one south of Priord Lake, and the smaller one in front of the snowfield west of Deadhorse Lake, may be active today. The tallest rock glacier termini stand 30 m high, thus the maximum thickness of these deposits is several tens of meters. Smiths Fork Till (late Pleistocene) – Unconsolidated, matrix-supported, poorly sorted diamicton deposited during the last glaciation (ca. 32,000 to 14,000 years ago) and considered correlative to the Pinedale Glaciation elsewhere in the Rocky Mountains. Inside the zone of tilted Paleozoic strata that forms a hogback encircling the Uinta Mountains, the diamicton consists of pebbles, cobbles, and boulders of Uinta Mountain Group lithologies, with abundant sandstone and quartzite boulders at the surface. Outside the hogback, limestone and sandstone clasts are common. Matrix varies from reddish-brown, fine silty clay in areas of exposed Tertiary sediment, to pink sand in areas dominated by the Uinta Mountain Group. Clasts are commonly angular to subrounded, especially the larger surface boulders. Striated clasts are locally abundant. Pockets of rounded clasts are also locally present, reflecting incorporation of proglacial outwash deposits during glacial advance. Surface topography is variable, ranging from smooth to hummocky with small ridges/knolls and kettles (some containing small ponds). Soils are generally poorly developed Inceptisols (A/Bw/C) with weak cambic horizons and only minor evidence for leaching of sesquioxides. As mapped, this unit includes end and lateral moraine complexes, as well as colluvium and mass wasting deposits along the foot of these moraines. Locally, units designated as Smiths Fork Till may also include outwash deposits, especially in areas where meltwater streams flowed through broad areas of hummocky end moraines. Sediment mapped as Smiths Fork Till was deposited during the last major glaciation in the Uinta Mountains, the Smiths Fork Glaciation. This material was deposited directly by glacier ice, either as basal meltout or lodgment till; englacial melt-out till; or supraglacial till deposited by melt-out, dumping off the ice surface, ice thrusting, ice ploughing, or by squeezing and deforming of saturated sediment by overlying glacier ice. This deposit may include till that has moved as mudflows, but not over significant distances (less than a few meters or tens of meters). Thickness of the sediment in the valley centers is on the order of 1 to 10 meters, while till thickness in the moraines may be as much as 50 m. Bedrock outcrops are absent or extremely rare. Because of the sandy material, this unit is well drained with a normally dry surface, except in the kettle depressions that are locally deep enough to intersect the water table. Till in the valley centers is generally quite stable due to low surface slopes and has a dense, compacted nature resulting from the weight of the overlying ice. Lateral moraines and till deposits on steeper bedrock slopes are prone to mass wasting, especially when water-saturated. Samples collected for cosmogenic 10 Be surface-exposure dating reveal that terminal moraines were abandoned by retreating glaciers before 16,000 years ago (Munroe and others, 2006; Laabs and others, 2007; Refsnider and others, 2008). Smiths Fork Outwash (late Pleistocene) – Unconsolidated, clast-supported cobble-gravel with local boulders and sand lenses, composed primarily of Uinta Mountain Group lithologies. Clasts are generally well rounded, and occasionally bear thin carbonate coatings and pendants in locations downstream from outcrops of the Paleozoic limestone units. Because of the coarse material, this unit is permeable and well drained. These sediments were deposited in high-energy glaciofluvial environments by meltwater draining from the terminal moraines of the Smiths Fork-age glaciers. Outwash surfaces form conspicuous valley trains extending downstream from all of the major terminal moraines. Original features of these surfaces, including braided channels and channel bars, can still be seen on aerial photos. Outwash surfaces related to the Smiths Fork glacial maximum were reworked or incised by glacial meltwater during retreat from the terminal moraines and also during the Holocene, forming a series of prominent terraces. Thickness is generally unknown, but is likely from 1 to 20 m. Pre-Smiths Fork Till, Undivided (middle or late Pleistocene) – Glacial diamicton similar in physical properties and composition to Smiths Fork Till, but located beyond the Smiths Fork glacial limit in a position where it is not possible to determine whether these sediments were deposited during the Blacks Fork or an earlier glaciation. This deposit displays a greater degree of soil development than Smiths Fork Till. Thickness is generally unknown, but may be as much as 50 m. Pre-Smiths Fork Outwash, Undivided (middle or late Pleistocene) – Outwash similar in physical properties and composition to Smiths Fork Outwash, but located above Smiths Fork-age outwash in a position where it is not possible to determine whether these sediments were deposited during the Blacks Fork or an earlier glaciation. This mapping unit also includes compound outwash surfaces where deposits of multiple glaciations have merged and cannot be distinguished. Thickness is generally unknown, but is likely from 1 to 20 m. Blacks Fork Till (middle or late Pleistocene) – Similar to Smiths Fork Till, but deposited during the penultimate Blacks Fork Glaciation. This event is likely correlative to the Bull Lake Glaciation, which occurred at approximately 160,000 to 130,000 years ago in the Yellowstone Plateau and Wind River Mountains regions, or possibly at 120,000 to 95,000 years ago. Soils on this material are generally thicker and more developed compared to Smiths Fork Till, and moraines composed of this material have more rounded crests and fewer large boulders on their surface. Thickness of till in valley centers is 1 to 10 meters, while thickness in moraines may be as much as 50 m. Blacks Fork Outwash (middle or late Pleistocene) – Similar to Smiths Fork Outwash, but found at higher elevations above the modern streams. Terraces are generally graded to Blacks Fork-age end moraines. Thickness is generally unknown, but is likely from 1 to 20 m. Pre-Blacks Fork Till (early[?] or middle Pleistocene) – Similar to Smiths Fork and Blacks Fork tills, except that the position of these deposits outside the Smiths Fork and Blacks Fork glacial limits indicates that they date to earlier in the Pleistocene. Thickness is generally less than that of Smiths Fork and Blacks Fork Till, but locally may be as much as 100 m as seen in the moraine in the Yellowstone River valley near Altonah, Utah. Pre-Blacks Fork Outwash (early[?] or middle Pleistocene) – Identical to Smiths Fork and Blacks Fork outwash except located at the highest elevations above modern streams and in positions adjacent to Pre-Blacks Fork Till. Thickness varies but is likely from 1 to 20 m. Thin Glacial Till Over Bedrock (Pleistocene) – Thin, unconsolidated deposits of till above a glacially-polished and/or striated or grooved bedrock ledge. Thickness ranges from a few meters of matrix-supported diamicton to a scattering of boulders on a bedrock surface. Polished bedrock is streamlined in places into small (meter scale) roches moutonnées and p-forms. Striations record multiple ice-flow directions in some localities. Overall surface topography of these units reflects strong control of underlying bedrock ledges. This deposit is found only in high basins where glacier erosion was intense and deposition was limited. As mapped, this unit includes thin regolith and colluvium, especially in areas where large amounts of shale are exposed in the cirque headwalls. In general, cirques at the western end of the mapping area tend to have better developed and more extensive areas of striated bedrock ledge. High elevation valley floors at the eastern end of the Uinta Mountains tend to be covered by a thin, but more continuous, layer of till interrupted by less common bedrock outcrops. Bedrock and Non-glacial Surficial Deposits (Phanerozoic and Proterozoic) – Well-consolidated sedimentary rocks and unconsolidated non-glacial surficial deposits of the Uinta Mountains. This unit includes non-glacial surficial deposits that are outside of the glaciated valleys and non-glacial surficial deposits that are within the glacial valleys but are too small or too thin to show on the map at this scale. GLACIAL SYMBOLS CONTACTS – Dashed where approximately located. ICE-MARGINAL CHANNELS – Drainages created or exploited by meltwater derived from valley glaciers. Most of these are associated with Smiths Fork-age end and lateral moraines, although some channels are associated with Blacks Fork and pre-Blacks Fork moraines. Many channels are occupied by underfit streams, although some are completely dry. All contain cobbles and small boulders that were transported by meltwater-enhanced flows. This lag is locally mantled by silty alluvium and colluvium that is well drained due to the permeability of the underlying coarser sediment. CIRQUE HEADWALLS – Prominent arcuate headwalls formed through glacial and periglacial erosion at the heads of valleys. MORAINE CRESTS – Crests of prominent end moraines and lateral moraines. Terminal and lateral moraines of the Smiths Fork Glaciation are most prominent due to their relatively young age. Blacks Fork-age terminal and lateral moraines are more subdued due to their longer period of weathering, including possibly more intense periglacial processes during the Smiths Fork Glaciation. The outer limit of a specific till unit was drawn at the foot of the distal moraine slope, so that moraine crests are shown slightly inside the maximum till extent. Prominent recessional moraines are also highlighted upstream from the terminal moraine complexes. Smiths Fork-age recessional moraines are generally smaller than the terminal moraines, and many have been extensively reworked by fluvial processes. SAMPLE LOCATIONS – Location of samples taken for cosmogenic dating. A table of the samples and their approximate ages is included with the Geographic Information System (GIS) files that support this map. INTRODUCTION This map represents the first complete inventory of the glacial deposits in the Uinta Mountains since Atwood (1909) described the glacial geology of this area. It is the result of previous and continuing work by the authors and others to better understand the glacial and climatic history of this fascinat- ing area. All areas were mapped at 1:24,000-scale on topographic maps and aerial photographs. Roaded areas were checked in the field, along with most areas accessible by foot (e.g., the High Uintas Wilderness Area). Munroe mapped the north flank of the Uinta Mountains between Leidy Peak and Utah Highway 150 from 1998 to 2000. Laabs mapped the south flank from Marsh Peak west to Wolf Creek Summit between 2002 and 2005. In 2006 this existing mapping was supplemented by additional fieldwork west of Utah Highway 150, including the West Fork Duchesne, South Fork Provo, Chalk Creek, and Beaver Creek drainages. During this time Munroe and Laabs combined their mapping of the north and south flanks, and integrated mapping by Oviatt (1994) and Refsnider (2006) to produce a unified map of glacial deposits for the Uinta Mountains region. The Miscellaneous Publication series provides non-UGS authors with a high-quality format for documents concerning Utah geology. Although review comments have been incorporated, this publication does not necessarily conform to UGS technical, editorial, or policy standards. The Utah Department of Natural Resources, Utah Geological Survey, makes no warranty, expressed or implied, regarding the suitability of this product for a particular use. The Utah Department of Natural Resources, Utah Geological Survey, shall not be liable under any circumstances for any direct, indirect, special, incidental, or consequential damages with respect to claims by users of this product. This geologic map was funded by the Utah Geological Survey and the USDA-USFS Ashley and Uinta-Wasatch-Cache National Forests. The views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U.S. Government. Persons or agencies using these data specifically agree not to misrepresent the data, nor to imply that changes they made were approved by the Utah Geological Survey, and should indicate the data source and any modifications made on plots, digital copies, derivative products, and in metadata. For use at 1:100,000 scale only. The Utah Geological Survey (UGS) does not guarantee accuracy or completeness of data. Base from U.S. Geological Survey 30' x 60' quadrangles Shaded relief derived from 10 meter National Elevation Dataset Lakes are from high-resolution National Hydrology Dataset. Lakes with areas less than 2000 m 2 are not shown Projection: UTM Zone 12 Datum: NAD 1927 Spheroid: Clarke 1866 Project Manager: Douglas A. Sprinkel (UGS) Cartographer: J. Buck Ehler (UGS) GIS Analysts: Lee B. Corbett (Middlebury College), J. Buck Ehler (UGS) ISBN 1-55791-925-2 This publication commemorates the 100th anniversary of Wallace Atwood's classic 1909 publication on glaciations of the Wasatch and Uinta Mountains. GLACIAL GEOLOGIC MAP OF THE UINTA MOUNTAINS AREA, UTAH AND WYOMING by Jeffrey S. Munroe 1 and Benjamin J.C. Laabs 2 1 Middlebury College, Geology Department, Middlebury, VT 05753 2 SUNY Geneseo, Department of Geological Sciences, 1 College Circle, Geneseo, NY 14454 2009 SCALE 1:100,000 CONTOUR INTERVAL 50 METERS CORRELATION OF MAP UNITS INDEX TO U.S. GEOLOGICAL SURVEY 30'x60' QUADRANGLES ACKNOWLEDGMENTS Glacial mapping of the Provo River drainage was adapted from Refsnider (2006). Mapping of the Weber River drainage was adapted from Oviatt (1994). Other sources of mapping information consulted during this project include Atwood (1909), Bryant (1992), and Carrara (1980). The field assistance of E. Carson, M. Devito, D. Douglass, D. Julio, O. Krawciw, N. Laabs, K. Lawson, J. Martin, L. Martin de Frutos, D. Mickelson, N. Oprandy, A. Rishavy, J. Shakun, and J. Silverman is greatly appreciated. Logistical support and assistance was provided by the Ashley National Forest and the Uinta-Wasatch-Cache National Forest. Special thanks to Darlene Koerner and Steve Ryberg. Support for our glacial mapping in the Uintas was provided by the U.S. Forest Service, University of Wisconsin-Madison, Geological Society of America, Desert Research Institute, Sigma Xi, Utah Geological Survey, and National Science Foundation EAR 0345112 and 0345277. We thank the following for their reviews of the map: Kurt Refsnider (University of Colorado-Boulder); Jack Oviatt (Kansas State University); and Douglas A. Sprinkel, Grant C. Willis, and Michael D. Hylland (Utah Geological Survey). We also thank J. Buck Ehler (Utah Geological Survey) and Ashley Corbett (Middlebury College) for their work on the GIS files. REFERENCES Atwood, W.W., 1909, Glaciation of the Uinta and Wasatch Mountains: U.S. Geological Survey Professional Paper 61, 96 p. Bradley, W.A., 1936, Geomorphology of the north flank of the Uinta Mountains: U.S. Geological Survey Professional Paper 185-I, p. 163-169. Bryant, B., 1992, Geologic and structure maps of the Salt Lake City 1° x 2° quadrangle, Utah and Wyoming: U.S. Geological Survey Miscellaneous Investigations Series Map I-1997, 3 plates, scale 1:125,000. Carrara, P.E., 1980, Surficial geologic map of the Vernal 1° x 2° quadrangle, Colorado and Utah: U.S. Geological Survey Miscellaneous Investigations Series Map I-1204, 1 plate, scale 1:250,000. Chadwick, O.A., Hall, R.D., and Phillips, F.M., 1997, Chronology of Pleistocene glacial advances in the central Rocky Mountains: Geological Society of America Bulletin, v. 109, no. 11, p. 1443-1452. Dahms, D., 2002, Glacial stratigraphy of Stough Creek basin, Wind River Range, Wyoming: Geomorphology, v. 42, no. 1, p. 59-83. Laabs, B.J.C., and Carson, E.C., 2005, Glacial geology of the southern Uinta Mountains, in Dehler, C.M., Pederson, J.L., Sprinkel, D.A., and Kowallis, B.J., editors, Uinta Mountain geology: Utah Geological Association Publication 33, p. 235-253. Laabs, B.J.C., Munroe, J.S., Rosenbaum, J.G., Refsnider, K.A., Mickelson, D.M., Singer, B.S., and Caffee, M.W., 2007, Chronology of the Last Glacial Maximum in the upper Bear River basin, Utah: Arctic, Antarctic and Alpine Research, v. 39, no. 4, p. 537-548. Laabs, B.J.C., Refsnider, K.A., Munroe, J.S., Mickelson, D.M., Applegate, P.J., Singer, B.S., and Caffee, M.W., 2009: Latest Pleistocene glacial chronology of the Uinta Mountains: Support for Moisture-Driven Asynchrony of the Last Deglaciation: Quaternary Science Reviews, v. 28, p. 1171-1187. Licciardi, J.M., and Pierce, K.L., 2008, Cosmogenic exposure-age chronologies of Pinedale and Bull Lake glaciations in greater Yellowstone and the Teton Range, USA: Quaternary Science Reviews, v. 27, p. 814-831. Munroe, J.S., Laabs, B.J.C., Shakun, J.D., Singer, B.S., Mickelson, D.M., Refsnider, K.A., and Caffee, M.W., 2006, Latest Pleistocene advance of alpine glaciers in the southwestern Uinta Mountains, Utah, USA—evidence for the influence of local moisture sources: Geology, v. 34, no. 10, p. 841-844. Oviatt, C.G., 1994, Quaternary geologic map of the upper Weber River drainage basin, Summit County, Utah: Utah Geological Survey Map 156, scale 1:50,000. Refsnider, K.A., 2006, Late Quaternary glacial and climate history of the Provo River drainage, Uinta Mountains, Utah: Madison, University of Wisconsin, M.S. thesis, 140 p. Refsnider, K.A., Laabs, B.J.C., and Mickelson, D.M., 2007, Glacial geology and equilibrium line altitude reconstructions for the Provo River drainage, Uinta Mountains, Utah, U.S.A.: Arctic, Antarctic, and Alpine Research, vol. 39, no. 4, p. 529-536. Refsnider, K.A., Laabs, B.J.C., Plummer, M.A., Mickelson, D.M., Singer, B.S., and Caffee, M.W., 2008, Last Glacial Maximum climate inferences from cosmogenic dating and glacier modeling of the western Uinta ice field, Uinta Mountains, Utah: Quaternary Research, v. 69, p. 130-144.vv Sharp, W.D., Ludwig, K.R., Chadwick, O.A., Amundson, R., and Glaser, L.L., 2003, Dating fluvial terraces by 230 Th/U on pedogenic carbonate, Wind River Basin, Wyoming: Quaternary Research, v. 59, p. 139-150. Plate 1 Utah Geological Survey Miscellaneous Publication 09-4DM Glacial Geologic Map of the Uinta Mountains Area UTAH GEOLOGICAL SURVEY a division of Utah Department of Natural Resources in cooperation with United States Forest Service Ñ EFBR-7 11 / ° 1 2 MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 2009 TRUE NORTH

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Page 1: glacial geologic map of the uinta mountains area, utah and wyoming

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10 0 105MILES

10 0 105KILOMETERS

Utah Geological Survey1594 West North Temple, Suite 3110

P.O. Box 146100, Salt Lake City, UT 84114-6100(801) 537-3300

geology.utah.govThis map was created from the Geographic Information System (GIS) data that accompanies this publication.

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10 0 105KILOMETERS

10 0 105MILES

SCALE 1:500,000

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SYNOPSIS OF GLACIAL HISTORYOver the past roughly two million years of Earth history, known as the Quaternary Period, numerous climatic

cycles led to the advance and retreat of glaciers worldwide. During each period of ice advance, or glaciation,global ice extent increased two- to three-fold and sea level fell more than 100 m as ocean water was stored asglacier ice on the continents. At high latitudes, ice sheets formed and expanded in North America and Eurasia toextents similar to or larger than that of the modern Antarctic ice sheet. Elsewhere, mountain glaciers advanced fardown valleys, even in ranges currently devoid of glaciers.

In the Uinta Mountains, a spectacular glacial landscape attests to the cumulative impact of these multipleglaciations during which erosion by ice produced numerous cirques, high basins, and U-shaped valleys, andenhanced the topographic relief between valleys and the high ridgelines. Some of the most impressive cirques inthe range include the large basin holding Red Castle Lake at the head of the East Fork Smiths Fork, and the basincontaining Walk-Up Lake at the head of the East Fork Whiterocks River. In places where cirques coalesced, broadbasins formed, such as Painter Basin, Brown Duck Basin, and the Grandaddy Lake area. The U-shaped crosssection of the Provo, Duchesne, and Bear River valleys can be seen from parts of the Mirror Lake Highway.

Material eroded from the core of the Uinta Mountains was deposited by ice and glacial meltwater at lowerelevations. Sediment deposited directly by glacier ice is called till, which can form ridges known as moraines thatoutline the lower margins of former glaciers. Some of the best preserved and most visible moraines in the UintaMountains are the sequence of sage- and Ponderosa pine-covered ridges impounding the Twin Pots Reservoirsouth of Moon Lake. Sediment deposited by glacial meltwater, known as outwash, is found downstream frommoraines and forms terraces above the modern rivers. Much of the Mirror Lake Highway south of Evanston,Wyoming, follows outwash of the Bear River. Lone Tree, Wyoming, is situated on a broad outwash surfacedeposited by meltwater from the Henrys Fork, West Fork Beaver Creek, and Middle Fork Beaver Creek glaciers.

Although geologic records from the oceans and ice sheets reveal that dozens of glaciations have occurredduring the Quaternary Period, terrestrial records of this time interval are dominated by the most recent glaciations,which obliterated or buried evidence of the older events. On this map, the “Qgo” and “Qgao” units markfragmentary evidence of older glaciations in the Uinta Mountains, such as the extensive lateral moraines andoutwash east of the Yellowstone River. Although the ages of these older glaciations are not known in the UintaMountains, similar deposits in the Wind River Range of Wyoming are older than a 660,000-year-old volcanic ash(Chadwick and others, 1997).

Deposits of the second-to-last glaciation, the Blacks Fork Glaciation, are more extensive. Prominent landformsof this event include lateral moraines along the Blacks Fork River north of Meeks Cabin Reservoir and along theeast side of the Yellowstone River. Although the age of this event has not been directly determined in the UintaMountains, recent work on correlative deposits of the Bull Lake Glaciation in northwestern Wyoming suggeststhat it occurred between 160,000 to 130,000 years ago, or possibly between 120,000 to 95,000 years ago(Chadwick and others, 1997; Sharp and others, 2003; Licciardi and Pierce, 2008).

The last glaciation in the Uinta Mountains is named the Smiths Fork Glaciation after the prominent terminalmoraine in the East Fork Smiths Fork valley (Bradley, 1936). Deposits of this event are widespread and the timingof the Smiths Fork Glaciation has been directly determined from geologic ages of moraines in several valleys.These results indicate that ice advance began about 32,000 years ago, culminated 25,000 years ago, and glaciersbegan retreating from their terminal moraines by 16,000 years ago. These results also indicate that the SmithsFork Glaciation occurred at essentially the same time as the Pinedale Glaciation elsewhere in the RockyMountains (Laabs and others, 2007, 2009).

The Uinta Mountains were largely ice free by 14,000 years ago, although moraines in some cirques and highbasins may represent glacial activity near the Pleistocene-Holocene transition. The highest moraines in the mostfavorably oriented cirques may also reflect more recent small-scale glacier activity. Although these moraineshave not been directly dated, similar deposits of this “Neoglacial” interval in the Wind River Range have beendated to the past 5,000 years (Dahms, 2002). Many of the rock glaciers in the Uinta Mountains also likely formedor were reactivated during this time interval.

DESCRIPTION OF THE ICE EXTENTS INSET MAPThis inset map displays reconstructed ice extents for the Smiths Fork Glaciation (ca. 32,000 to 14,000 years ago)

in the Uinta Mountains, determined through field observations coupled with interpretation of maps and aerialphotographs. Upper ice limits were defined by inflection points in cirque headwalls, and trimlines. Lower ice limitswere identified primarily by moraines, and by heads of outwash and ice-marginal channels. The western part of theUinta Mountains was occupied by numerous small cirque and valley glaciers, along with the relatively broad WesternUintas Ice Field (Refsnider and others, 2007). This ice field inundated the crest of the range (except for the highestpeaks) and drained into the Bear River, Weber River, Beaver Creek, North Fork Provo River, North Fork Duchesne,and Rock Creek valleys. The largest discrete valley glaciers developed in the central part of the Uinta Mountainswhere they flowed south and extended beyond the mountain front. Particularly large glaciers in the Lake Fork,Yellowstone, and Uinta River valleys were fed by broad, but confined, ice fields. In contrast, on the north slope of theUinta Mountains ice advanced from numerous north-draining cirques to form long, narrow, valley glaciers. Glaciersin the Blacks Fork, Smiths Fork, and Henrys Fork valleys extended beyond the range front. In the West and MiddleFork Beaver Creeks, Thompson Creek, and Burnt Fork valleys, glaciers terminated at, or just south of, therange-bounding hogback. Glaciers in the Sheep Creek and Carter Creek valleys formed piedmont lobes on the northflank, south of the hogback. The smallest valley glaciers were found in the eastern part of the Uinta Mountains, whereice was entirely confined to valleys.

The formation of few relatively large glaciers in southern valleys compared to several smaller glaciers in northernvalleys is likely related to bedrock structure. Atwood (1909) suggested that gently-dipping bedrock on the south flankallowed Pleistocene glaciers to erode laterally more efficiently than glaciers on the north flank, leading to theformation of broad valleys at the heads of the Rock Creek, Lake Fork, Yellowstone, and Uinta River valleys. Thefloors of these valleys are above the estimated Smiths Fork-age equilibrium-line altitude (~3000 to 3100 m asl) forthe central part of the range (Laabs and Carson, 2005), adding support for the notion that these large glaciers weresustained by broad accumulation areas. Alternatively, the formation of relatively large glaciers in south-centralvalleys may be due to climatic differences. Laabs and others (2007) proposed that regional southwest-to-northeastcirculation during the Smiths Fork Glaciation may have delivered moisture-laden air masses to the southern part ofthe range, producing an orographic precipitation shadow over the northern valleys.

There is also evidence for a longitudinal precipitation gradient running parallel to the range axis. As noted byMunroe and others (2006), glaciers in the western part of the Uinta Mountains extended to lower elevations and hadequilibrium-line altitudes as low as 2600 m, which is ~600 m lower than glaciers farther east (~3200 m asl). Thispattern reflects a tremendous enhancement of the modern asymmetric precipitation pattern in the Uinta Mountains,likely driven by the presence of pluvial Lake Bonneville, which was located within 60 km of the western UintaMountains and may have amplified precipitation in areas downwind.

DESCRIPTION OF MAP UNITSAlluvium (Holocene) – Unconsolidated deposits of moderately to well-sorted and stratified clastic sediments, including gravel, sand, silt, and clay, formed by deposition in moving water. Stratigraphy consists of well-rounded clasts usually mantled by thin (< 1 m) finer-grained overbank

deposits. The modern floodplain is inset within both glacial till and outwash deposits and wet and dry meadows are abundant. The present location and condition of the river or stream channel reflect the influence of postglacial disturbances including mass movements, Neoglacialactivity, and human perturbations, including diversions and logging. Thickness is typically less than 10 m. Although alluvium is ubiquitous along modern streams, only the broadest and most continuous areas of alluvium are shown on the map.

Alluvial-Fan Deposits (Holocene) – Unconsolidated, poorly to moderately sorted boulder-gravel, sand, silt, and clay. The lithology and grain size of the material comprising the fans reflects the rocks in the fan source area. For example, clay and silt derived from the Red Pine Shaledominate the large fan near the East Fork Blacks Fork Guard Station (section 23, T. 2 N., R. 12 E., Salt Lake Base Line and Meridian). Coarser boulders and gravel from the Bishop Conglomerate and Quaternary glacial deposits comprise the fan west of Meeks Cabin Reservoir inthe Blacks Fork drainage (section 21, T. 3 N., R. 12 E., Salt Lake Base Line and Meridian). The alluvial fan below Dry Canyon in the Lake Fork drainage (section 24, T. 2 N., R. 6 W., Uinta Base Line and Meridian) is composed of coarse-grained sand and cobbles of Uinta MountainGroup quartzite derived from the Duchesne River Formation.Fans with a radial pattern of surface drainage extend outward from the base of a steep channel or chute cut through a lateral moraine or down a valley wall. Fans with hummocky surface topography owing to deposition primarily by mass wasting rather than alluvial activity arecommon below chutes, whereas fans with smooth surfaces are common below steep fluvial channels. Fan formation occurred through a combination of post-glacial fluvial and colluvial processes. Alluvial fans were mapped separately from cones of coarse, blocky debris producedby rockfall, which were mapped with talus (Qmt) and slides, slumps, and flows (Qms).Fan formation is apparently an episodic process linked to climatic factors including rate of snowmelt and rainfall. A single entrenched stream, reflecting relative stability, occupies many modern fans. However, bars and shallow channels visible on unvegetated fans (e.g., west ofMeeks Cabin Reservoir) are evidence of past floods across the fan surface. Disturbances linked to fan progradation include the damming of the Stillwater Fork Bear River to produce Christmas Meadows (section 15, T. 1 N., R. 10 E., Salt Lake Base Line and Meridian), andimpoundment of the Lake Fork River to form the pre-dam Moon Lake (section 18, T. 2 N., R. 5 W., Uinta Base Line and Meridian). Variable thickness from 1 to more than 10 m.

Lacustrine Deposits (Holocene) – Unconsolidated lacustrine sediments, including laminated fine sand, silt and clay, and fine colluvium. Buried organic layers are also common. This deposit is commonly found in formerly closed depressions dammed by end moraines, till ridges,hummocks, and mass-wasting deposits. These basins are now marked by wet meadows and/or small lakes. Along major rivers, the landforms associated with this deposit are commonly distinguished by an abrupt change in channel sinuosity. Only the larger deposits are mapped; inareas of hummocky moraine or stagnant ice topography smaller versions of this deposit are ubiquitous.

Christmas Meadows in the Stillwater Fork is a drained lake basin where water was temporarily impounded behind a set of alluvial fans. The large meadow below the ford on the West ForkBlacks Fork is impounded behind a recessional moraine complex. In the Middle Fork Blacks Fork a wet meadow marks the extent of a drained lake basin that was impounded behind slumpdeposits derived from the western valley wall. Cow Park and Little Meadow above Fish Creek are other examples of these deposits. Thickness is generally unknown, but may locally exceed10 m.

Slides, Slumps, and Flows (Holocene and Pleistocene [?]) – Unconsolidated, poorly sorted deposits of locally derived material that has moved down slope through landsliding, slumping, andflowing. Individual headscarps and rotated blocks can often be identified, and sag ponds are locally present where blocks are back-rotated (e.g., west side of Middle Fork Blacks Fork). Smallmudflows and debris flows are common at the base of the scarps. The majority of slumps are located along the oversteepened sides of glaciated valleys where they are obviously post-glacialfeatures.The mapped slumps and landslides on the north slope typically involve the Tertiary Wasatch Formation and overlying Bishop Conglomerate. Pleistocene glacial deposits are alsoincorporated where slumps occur along glaciated valley sides. Across the south slope, landslides are common along the bedrock contact between the Mississippian Doughnut (shale) andHumbug (limestone and sandstone) Formations. In some places, tributary valleys may have been dammed by lateral moraines and were subsequently filled by lakes. Failure of lateralmoraine-dammed lakes may have instigated landslides in Lake Fork and Yellowstone canyons. Thickness is variable, but may exceed 100 m.

Talus Deposits (Holocene and Pleistocene [?]) – Unconsolidated, poorly sorted deposits of angular boulders located at the base of cirque headwalls and along glacial valleysides. Blocks are detached from bedrock outcrops by freeze-thaw cycles, heavy rain, and snow avalanching. The surfaces of talus deposits are extremely coarse with fineshaving been removed by nival meltwater. Accumulations of fine colluvium are common down slope from many talus features, especially in settings below cliffs containinga large component of shale. Small, vegetated ridges of fine-grained material are present at the toe of many talus slopes, suggesting that the talus may be slowly movingoutward from the source area.As mapped, talus deposits include broad sheet-like slopes, discrete avalanche cones, and series of coalesced cones, protalus ramparts, slushflow levee/channel complexes,small lobate rock glaciers, and small end moraines.In glaciated valleys, talus is post-glacial and presumably accumulated during more severe periglacial conditions in the latest Pleistocene. Some of the features may have beenreactivated during the late Holocene Neoglacial period. Some talus deposits are active today, as evidenced by observed rock fall and fresh, lichen-free rocks. Thickness isgenerally unknown, but likely 1 to 50 m.

Rock Glacier Deposits (Holocene and Pleistocene [?]) – Unconsolidated, poorly sorted deposits of angular boulders having a characteristic surfacemorphology owing to flow through deformation of interstitial ice. Fines are more common in these features than in talus, perhaps due to comminutionof rock during movement or accumulation of eolian sediment. Fines may also be derived from shale layers exposed in the valley walls above the rockglacier, and may decrease the permeability of the talus sufficiently to allow formation of interstitial ice leading to rock glacier genesis.In plan view, rock glaciers take the form of lobate bulges extending outward from more uniform talus slopes, and of tongue-like masses occupying thefloor of high-altitude cirque basins. Transverse ridges and furrows are common on rock glacier surfaces, indicating collapse of underlying zones ofincreased ice content during melt-out. Unstable, lichen-free, steep frontal slopes, and other features indicative of contemporary activity includingsurface meltwater ponds, are present on many of these features. Other rock glaciers, including most of those located along valley sides, appear to bestabilized, with gentler frontal slopes and greater lichen cover.

Because of their locations within the glaciated valleys, all mapped rock glaciers are post-glacial in age. The exact timing of theirformation is unknown, although it is likely that many of them formed in the latest Pleistocene and were reactivated during theNeoglaciation. Several rock glaciers in the study area, including the large one south of Priord Lake, and the smaller one in front of thesnowfield west of Deadhorse Lake, may be active today. The tallest rock glacier termini stand 30 m high, thus the maximum thickness ofthese deposits is several tens of meters.

Smiths Fork Till (late Pleistocene) – Unconsolidated, matrix-supported, poorly sorted diamicton deposited during the last glaciation (ca.32,000 to 14,000 years ago) and considered correlative to the Pinedale Glaciation elsewhere in the Rocky Mountains. Inside the zone oftilted Paleozoic strata that forms a hogback encircling the Uinta Mountains, the diamicton consists of pebbles, cobbles, and boulders of

Uinta Mountain Group lithologies, with abundant sandstone and quartzite boulders at the surface. Outside the hogback,limestone and sandstone clasts are common. Matrix varies from reddish-brown, fine silty clay in areas of exposed Tertiarysediment, to pink sand in areas dominated by the Uinta Mountain Group. Clasts are commonly angular to subrounded,especially the larger surface boulders. Striated clasts are locally abundant. Pockets of rounded clasts are also locally present,reflecting incorporation of proglacial outwash deposits during glacial advance. Surface topography is variable, ranging fromsmooth to hummocky with small ridges/knolls and kettles (some containing small ponds). Soils are generally poorlydeveloped Inceptisols (A/Bw/C) with weak cambic horizons and only minor evidence for leaching of sesquioxides.As mapped, this unit includes end and lateral moraine complexes, as well as colluvium and mass wasting deposits along thefoot of these moraines. Locally, units designated as Smiths Fork Till may also include outwash deposits, especially in areaswhere meltwater streams flowed through broad areas of hummocky end moraines.Sediment mapped as Smiths Fork Till was deposited during the last major glaciation in the Uinta Mountains, the Smiths ForkGlaciation. This material was deposited directly by glacier ice, either as basal meltout or lodgment till; englacial melt-out till;or supraglacial till deposited by melt-out, dumping off the ice surface, ice thrusting, ice ploughing, or by squeezing anddeforming of saturated sediment by overlying glacier ice. This deposit may include till that has moved as mudflows, but notover significant distances (less than a few meters or tens of meters). Thickness of the sediment in the valley centers is on theorder of 1 to 10 meters, while till thickness in the moraines may be as much as 50 m. Bedrock outcrops are absent orextremely rare. Because of the sandy material, this unit is well drained with a normally dry surface, except in the kettledepressions that are locally deep enough to intersect the water table. Till in the valley centers is generally quite stable due tolow surface slopes and has a dense, compacted nature resulting from the weight of the overlying ice. Lateral moraines andtill deposits on steeper bedrock slopes are prone to mass wasting, especially when water-saturated. Samples collected forcosmogenic 10Be surface-exposure dating reveal that terminal moraines were abandoned by retreating glaciers before 16,000years ago (Munroe and others, 2006; Laabs and others, 2007; Refsnider and others, 2008).

Smiths Fork Outwash (late Pleistocene) – Unconsolidated, clast-supported cobble-gravel with local boulders and sand lenses,composed primarily of Uinta Mountain Group lithologies. Clasts are generally well rounded, and occasionally bear thincarbonate coatings and pendants in locations downstream from outcrops of the Paleozoic limestone units. Because of thecoarse material, this unit is permeable and well drained.

These sediments were deposited in high-energy glaciofluvial environments by meltwater draining from the terminal moraines of the SmithsFork-age glaciers. Outwash surfaces form conspicuous valley trains extending downstream from all of the major terminal moraines. Originalfeatures of these surfaces, including braided channels and channel bars, can still be seen on aerial photos. Outwash surfaces related to the SmithsFork glacial maximum were reworked or incised by glacial meltwater during retreat from the terminal moraines and also during the Holocene,forming a series of prominent terraces. Thickness is generally unknown, but is likely from 1 to 20 m.

Pre-Smiths Fork Till, Undivided (middle or late Pleistocene) – Glacial diamicton similar in physical properties and composition to Smiths Fork Till, but locatedbeyond the Smiths Fork glacial limit in a position where it is not possible to determine whether these sediments were deposited during the Blacks Fork or an earlierglaciation. This deposit displays a greater degree of soil development than Smiths Fork Till. Thickness is generally unknown, but may be as much as 50 m.

Pre-Smiths Fork Outwash, Undivided (middle or late Pleistocene) – Outwash similar in physical properties and composition to Smiths Fork Outwash, but located above SmithsFork-age outwash in a position where it is not possible to determine whether these sediments were deposited during the Blacks Fork or an earlier glaciation. This mapping unit alsoincludes compound outwash surfaces where deposits of multiple glaciations have merged and cannot be distinguished. Thickness is generally unknown, but is likely from 1 to 20 m.

Blacks Fork Till (middle or late Pleistocene) – Similar to Smiths Fork Till, but deposited during the penultimate Blacks Fork Glaciation. This event is likely correlative to the Bull LakeGlaciation, which occurred at approximately 160,000 to 130,000 years ago in the Yellowstone Plateau and Wind River Mountains regions, or possibly at 120,000 to 95,000 years ago.Soils on this material are generally thicker and more developed compared to Smiths Fork Till, and moraines composed of this material have more rounded crests and fewer largeboulders on their surface. Thickness of till in valley centers is 1 to 10 meters, while thickness in moraines may be as much as 50 m.

Blacks Fork Outwash (middle or late Pleistocene) – Similar to Smiths Fork Outwash, but found at higher elevations above the modern streams. Terraces are generally graded to Blacks Fork-age endmoraines. Thickness is generally unknown, but is likely from 1 to 20 m.

Pre-Blacks Fork Till (early[?] or middle Pleistocene) – Similar to Smiths Fork and Blacks Fork tills, except that the position of these deposits outside the Smiths Fork and Blacks Fork glacial limitsindicates that they date to earlier in the Pleistocene. Thickness is generally less than that of Smiths Fork and Blacks Fork Till, but locally may be as much as 100 m as seen in the moraine in theYellowstone River valley near Altonah, Utah.

Pre-Blacks Fork Outwash (early[?] or middle Pleistocene) – Identical to Smiths Fork and Blacks Fork outwash except located at the highest elevations above modern streams and in positions adjacent toPre-Blacks Fork Till. Thickness varies but is likely from 1 to 20 m.

Thin Glacial Till Over Bedrock (Pleistocene) – Thin, unconsolidated deposits of till above a glacially-polished and/or striated or grooved bedrock ledge. Thickness ranges from a few meters of matrix-supported diamicton to a scattering ofboulders on a bedrock surface. Polished bedrock is streamlined in places into small (meter scale) roches moutonnées and p-forms. Striations record multiple ice-flow directions in some localities. Overall surface topography of these unitsreflects strong control of underlying bedrock ledges. This deposit is found only in high basins where glacier erosion was intense and deposition was limited.As mapped, this unit includes thin regolith and colluvium, especially in areas where large amounts of shale are exposed in the cirque headwalls. In general, cirques at the western end of the mapping area tend to have better developed andmore extensive areas of striated bedrock ledge. High elevation valley floors at the eastern end of the Uinta Mountains tend to be covered by a thin, but more continuous, layer of till interrupted by less common bedrock outcrops.

Bedrock and Non-glacial Surficial Deposits (Phanerozoic and Proterozoic) – Well-consolidated sedimentary rocks and unconsolidated non-glacial surficial deposits of the Uinta Mountains. This unit includes non-glacial surficial depositsthat are outside of the glaciated valleys and non-glacial surficial deposits that are within the glacial valleys but are too small or too thin to show on the map at this scale.

GLACIAL SYMBOLSCONTACTS – Dashed where approximately

located.

ICE-MARGINAL CHANNELS – Drainagescreated or exploited by meltwater derivedfrom valley glaciers. Most of these areassociated with Smiths Fork-age end andlateral moraines, although some channels areassociated with Blacks Fork and pre-BlacksFork moraines. Many channels are occupiedby underfit streams, although some arecompletely dry. All contain cobbles andsmall boulders that were transported bymeltwater-enhanced flows. This lag islocally mantled by silty alluvium andcolluvium that is well drained due to thepermeability of the underlying coarsersediment.

CIRQUE HEADWALLS – Prominent arcuateheadwalls formed through glacial andperiglacial erosion at the heads of valleys.

MORAINE CRESTS – Crests of prominentend moraines and lateral moraines. Terminaland lateral moraines of the Smiths ForkGlaciation are most prominent due to theirrelatively young age. Blacks Fork-ageterminal and lateral moraines are moresubdued due to their longer period ofweathering, including possibly more intenseperiglacial processes during the Smiths ForkGlaciation. The outer limit of a specific tillunit was drawn at the foot of the distalmoraine slope, so that moraine crests areshown slightly inside the maximum tillextent. Prominent recessional moraines arealso highlighted upstream from the terminalmoraine complexes. Smiths Fork-agerecessional moraines are generally smallerthan the terminal moraines, and many havebeen extensively reworked by fluvialprocesses.

SAMPLE LOCATIONS – Location ofsamples taken for cosmogenic dating. Atable of the samples and their approximateages is included with the GeographicInformation System (GIS) files that supportthis map.

INTRODUCTIONThis map represents the first complete inventory of the glacial deposits in the Uinta Mountains since Atwood (1909) described the glacial geology of this area. It is the result of previous and continuing work by the authors and others to better understand the glacial and climatic history of this fascinat-ing area. All areas were mapped at 1:24,000-scale on topographic maps and aerial photographs. Roaded areas were checked in the field, along with most areas accessible by foot (e.g., the High Uintas Wilderness Area). Munroe mapped the north flank of the Uinta Mountains between Leidy Peakand Utah Highway 150 from 1998 to 2000. Laabs mapped the south flank from Marsh Peak west to Wolf Creek Summit between 2002 and 2005. In 2006 this existing mapping was supplemented by additional fieldwork west of Utah Highway 150, including the West Fork Duchesne, South Fork

Provo, Chalk Creek, and Beaver Creek drainages. During this time Munroe and Laabs combined their mapping of the north and south flanks, and integrated mapping by Oviatt (1994) and Refsnider (2006) to produce a unified map of glacial deposits for the Uinta Mountains region.

The Miscellaneous Publication series provides non-UGS authors with a high-quality format for documents concerning Utah geology. Although review comments have been incorporated, this publication does not necessarily conformto UGS technical, editorial, or policy standards. The Utah Department of Natural Resources, Utah Geological Survey, makes no warranty, expressed or implied, regarding the suitability of this product for a particular use. The UtahDepartment of Natural Resources, Utah Geological Survey, shall not be liable under any circumstances for any direct, indirect, special, incidental, or consequential damages with respect to claims by users of this product.

This geologic map was funded by the Utah Geological Survey and the USDA-USFS Ashley and Uinta-Wasatch-Cache National Forests. The views and conclusions contained in this document are those of the authors and should notbe interpreted as necessarily representing the official policies, either expressed or implied, of the U.S. Government.

Persons or agencies using these data specifically agree not to misrepresent the data, nor to imply that changes they made were approved by the Utah Geological Survey, and should indicate the data source and any modificationsmade on plots, digital copies, derivative products, and in metadata.

For use at 1:100,000 scale only. The Utah Geological Survey (UGS) does not guarantee accuracy or completeness of data.

Base from U.S. Geological Survey 30' x 60' quadranglesShaded relief derived from 10 meter National Elevation Dataset

Lakes are from high-resolution National Hydrology Dataset. Lakes with areas less than 2000 m2 are not shownProjection: UTM Zone 12

Datum: NAD 1927Spheroid: Clarke 1866

Project Manager: Douglas A. Sprinkel (UGS)Cartographer: J. Buck Ehler (UGS)

GIS Analysts: Lee B. Corbett (Middlebury College), J. Buck Ehler (UGS)ISBN 1-55791-925-2

This publication commemorates the 100th anniversary of Wallace Atwood'sclassic 1909 publication on glaciations of the Wasatch and Uinta Mountains.

GLACIAL GEOLOGIC MAP OF THE UINTA MOUNTAINS AREA,UTAH AND WYOMING

byJeffrey S. Munroe1 and Benjamin J.C. Laabs2

1Middlebury College, Geology Department, Middlebury, VT 057532SUNY Geneseo, Department of Geological Sciences, 1 College Circle, Geneseo, NY 14454

2009

SCALE 1:100,000CONTOUR INTERVAL 50 METERS

CORRELATION OF MAP UNITS

INDEX TO U.S. GEOLOGICAL SURVEY 30'x60' QUADRANGLES

ACKNOWLEDGMENTSGlacial mapping of the Provo River drainage was

adapted from Refsnider (2006). Mapping of the WeberRiver drainage was adapted from Oviatt (1994). Othersources of mapping information consulted during thisproject include Atwood (1909), Bryant (1992), and Carrara(1980).

The field assistance of E. Carson, M. Devito, D.Douglass, D. Julio, O. Krawciw, N. Laabs, K. Lawson, J.Martin, L. Martin de Frutos, D. Mickelson, N. Oprandy, A.Rishavy, J. Shakun, and J. Silverman is greatly appreciated.

Logistical support and assistance was provided by theAshley National Forest and the Uinta-Wasatch-CacheNational Forest. Special thanks to Darlene Koerner andSteve Ryberg.

Support for our glacial mapping in the Uintas wasprovided by the U.S. Forest Service, University ofWisconsin-Madison, Geological Society of America,Desert Research Institute, Sigma Xi, Utah GeologicalSurvey, and National Science Foundation EAR 0345112and 0345277.

We thank the following for their reviews of the map:Kurt Refsnider (University of Colorado-Boulder); JackOviatt (Kansas State University); and Douglas A. Sprinkel,Grant C. Willis, and Michael D. Hylland (Utah GeologicalSurvey). We also thank J. Buck Ehler (Utah GeologicalSurvey) and Ashley Corbett (Middlebury College) for theirwork on the GIS files.

REFERENCESAtwood, W.W., 1909, Glaciation of the Uinta and Wasatch Mountains: U.S. Geological Survey Professional Paper 61, 96 p.Bradley, W.A., 1936, Geomorphology of the north flank of the Uinta Mountains: U.S. Geological Survey Professional Paper 185-I, p. 163-169.Bryant, B., 1992, Geologic and structure maps of the Salt Lake City 1° x 2° quadrangle, Utah and Wyoming: U.S. Geological Survey Miscellaneous Investigations Series Map

I-1997, 3 plates, scale 1:125,000.Carrara, P.E., 1980, Surficial geologic map of the Vernal 1° x 2° quadrangle, Colorado and Utah: U.S. Geological Survey Miscellaneous Investigations Series Map I-1204, 1

plate, scale 1:250,000.Chadwick, O.A., Hall, R.D., and Phillips, F.M., 1997, Chronology of Pleistocene glacial advances in the central Rocky Mountains: Geological Society of America Bulletin, v.

109, no. 11, p. 1443-1452.Dahms, D., 2002, Glacial stratigraphy of Stough Creek basin, Wind River Range, Wyoming: Geomorphology, v. 42, no. 1, p. 59-83.Laabs, B.J.C., and Carson, E.C., 2005, Glacial geology of the southern Uinta Mountains, in Dehler, C.M., Pederson, J.L., Sprinkel, D.A., and Kowallis, B.J., editors, Uinta

Mountain geology: Utah Geological Association Publication 33, p. 235-253.Laabs, B.J.C., Munroe, J.S., Rosenbaum, J.G., Refsnider, K.A., Mickelson, D.M., Singer, B.S., and Caffee, M.W., 2007, Chronology of the Last Glacial Maximum in the

upper Bear River basin, Utah: Arctic, Antarctic and Alpine Research, v. 39, no. 4, p. 537-548.Laabs, B.J.C., Refsnider, K.A., Munroe, J.S., Mickelson, D.M., Applegate, P.J., Singer, B.S., and Caffee, M.W., 2009: Latest Pleistocene glacial chronology of the Uinta

Mountains: Support for Moisture-Driven Asynchrony of the Last Deglaciation: Quaternary Science Reviews, v. 28, p. 1171-1187.Licciardi, J.M., and Pierce, K.L., 2008, Cosmogenic exposure-age chronologies of Pinedale and Bull Lake glaciations in greater Yellowstone and the Teton Range, USA:

Quaternary Science Reviews, v. 27, p. 814-831.Munroe, J.S., Laabs, B.J.C., Shakun, J.D., Singer, B.S., Mickelson, D.M., Refsnider, K.A., and Caffee, M.W., 2006, Latest Pleistocene advance of alpine glaciers in the

southwestern Uinta Mountains, Utah, USA—evidence for the influence of local moisture sources: Geology, v. 34, no. 10, p. 841-844.Oviatt, C.G., 1994, Quaternary geologic map of the upper Weber River drainage basin, Summit County, Utah: Utah Geological Survey Map 156, scale 1:50,000.Refsnider, K.A., 2006, Late Quaternary glacial and climate history of the Provo River drainage, Uinta Mountains, Utah: Madison, University of Wisconsin, M.S. thesis, 140 p.Refsnider, K.A., Laabs, B.J.C., and Mickelson, D.M., 2007, Glacial geology and equilibrium line altitude reconstructions for the Provo River drainage, Uinta Mountains,

Utah, U.S.A.: Arctic, Antarctic, and Alpine Research, vol. 39, no. 4, p. 529-536.Refsnider, K.A., Laabs, B.J.C., Plummer, M.A., Mickelson, D.M., Singer, B.S., and Caffee, M.W., 2008, Last Glacial Maximum climate inferences from cosmogenic dating

and glacier modeling of the western Uinta ice field, Uinta Mountains, Utah: Quaternary Research, v. 69, p. 130-144.vvSharp, W.D., Ludwig, K.R., Chadwick, O.A., Amundson, R., and Glaser, L.L., 2003, Dating fluvial terraces by 230Th/U on pedogenic carbonate, Wind River Basin, Wyoming:

Quaternary Research, v. 59, p. 139-150.

Plate 1Utah Geological Survey Miscellaneous Publication 09-4DM

Glacial Geologic Map of the Uinta Mountains AreaUTAH GEOLOGICAL SURVEYa division ofUtah Department of Natural Resourcesin cooperation withUnited States Forest Service

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