bluuebunny/crossref_metadata_2025_split huggingface dataset:
Precambrian metamorphic rocks of the Devil’s Gate- Weber Canyon area, northern Utah
Authors: DeCourten Frank L. 
Published: November 2007

Abstract
The site discussed here in is located in the central Wasatch Mountains near the mouth of Weber Canyon, 9 mi (15 km) southeast of Ogden, Utah. Numerous excellent exposures of Precambrian metamorphic and igneous rocks occur in Weber Canyon from approximately Mountain Green, Utah, downstream to the mouth, in an area of roughly 4 mi2 (10.5 km2) (Fig. 1). The area of principal interest is in sections 26 and 36, T.5N., R. 1 W., and in Sec. 28–32, T.5N., R. 1 E. (Salt Lake Meridian). The Devil’s Gate-Weber Canyon locality occupies the southwest comerof the Snow Basin 7½-minute Quadrangle andthe southeast corner of the Ogden, Utah 7½-minute Quadrangle. I-84 bisects the area and offers easy accessto many excellent outcrops.
Multiple soils in pre-Wisconsin drift on Mokowan Butte, southwestern Alberta
Authors: Karlstrom Eric T. 
Published: November 2007

Abstract
The stratigraphy and morphology of superposed pre-Wisconsin soils on Flaxville surface remnants (Alden, 1932) east of Waterton-Glacier Park can best be studed at Mokowan Butte (Fig. 1). The site is located on private land about 1.2 mi (1.9 km) east of the Waterton Park boundary and 3.6 mi (5.8 km) north ofthe International Boundary and is reached by driving about 21 mi (33.6 km) west of Cardston, Alberta, on a dirt road. The trip can be completed in a half day with a robust two-wheel or four-wheel drive vehicle. Landowners’ permission is not required.
The House Range, western Utah
Authors: Hintze Lehi F. , Robison Richard A. 
Published: November 2007

Abstract
The House Range is one of the principal ranges in western Utah (Fig. 1). It trends north-south for 60 mi (100 km)along the west edge of the Sevier Desert and lies 40 mi (65 km) west of Delta, Utah. The range has an asymmetric profile Its eastern slopes, formed mostly on dipslopes of Cambrian strata, rise gradually up from the Sevier Desert floor; its western face, formed by block faulting, rises abruptly from the floor of Tule Valley (also known as White Valley) at an elevation of 4,400 ft (1,300 m) to its highest point, Notch Peak, elevation 9,655 ft (2,943 m). The northwest face of Notch Peak forms one of the tallest sheer cliffs in the west.
Delta, an irrigation-farming community situated in the center of the Sevier Desert, is the nearest source of gas, food, and supplies. U.S. 6-50 cuts southwestward from Delta to cross the southern part of the House Range at Skull Rock Pass. Graded gravel roads extend the entire length of the range on either side; roads cross the range only at Skull Rock Pass, at Marjum Pass in the middle, and at Death (Dome) Canyon a few miles north of Marjum Pass.
People planning to visit the House Range should inquire in Delta about road conditions. Although most of the time the main gravel roads are suitable even for passenger cars, after storms these roads may be washed out and passable only with fourwheel-drive vehicles.
Stratigraphy and structure of the San Rafael Reef, Utah; A major monocline of the Colorado Plateau
Authors: Rigby J. Keith 
Published: November 2007

Abstract
Location. The San Rafael Swell is a major domal uplift in the northwestern Colorado Plateau and dominates the structure of east-central Utah. The San Rafael Reef site is on its eastern edge, approximately 13 mi (21 km) west of Green River, in Emery County, Utah (Fig. 1). 1–70 cuts more or less directly across the structure (Rigby and others, 1974).
Accessibility. Roadcuts are on right-of-way controlled by the Utah State Highway Commission. Land along side the route is generally controlled by the U.S. Bureau of Land Management.Alluvial flats along the San Rafael River are on private land.
Significance of Site. The San Rafael Swell is characteristic of many asymmetric large uplifts of the Colorado Plateau; and itseastern margin, the San Rafael Reef, is representative of monocline of the province. A complete stratigraphic sequence from the Permian White Rim-Cedar Mesa Sandstone up through Triassicand Jurassic rocks to the lower part of the Cretaceus Mancos Shale Fig. 2 is exposed along the highway. These rocks accumulated in a wide variety of depositional enviroments, ranging from marine carbonate and elastic environments to deserts(Rigby, 1978).
Moab salt-intruded anticline, east-central Utah
Authors: Baars D. L. , Doelling H. H. 
Published: November 2007

Abstract
Moab, Utah, lies on the northwestern end of the Moab Valley salt-intruded anticline on the banks of the Colorado River in east-central Utah, in T.25 and 26S., R.21 E. (38°36'N.,109°32'W.), on the Moab 15’ Quadrangle, in southern Grand County, Utah (Fig. 1). U.S. 163 passes through Moab and along the length of Moab Valley. The elevation at Moab is 4,000 ft(1,467 m). The area is readily accessible with any vehicle, but off-pavement lands are almost entirely privately owned and permission should be secured for specific locality access.
Kolob Canyons, Utah
Authors: Grant Sheldon Kerry 
Published: November 2007

Abstract
The site encompasses that portion of the Kolob Canyon ssection of Zion National Park, in southwestern Utah, that is visible from the 5-mi-long (8-km) park highway (Fig. 1). The park road is suitable for passenger cars and other vehicles.
Kolob Canyons offer spectacular views of slopes that show the effects of erosion on the thick massive Navajo Sandstone. In addition, exposures in Taylor Creek, LaVerkin Creek, and their tributaries reveal details of stratigraphy and structure. Much of the Mesozoic section is exposed, from the basal Timpoweap Limestone of Early Triassic age to the Jurassic Carmel Formation, inaccessible at the tops of the Navajo cliffs. Structurally, two episodes of tectonic activity’ are evident. The Late Cretaceus Sevier orogeny produced the Kanarra fold, with effects throughout the site. Most interesting perhaps is the Taylor Creek thrust zone, on the eastern limb of this fold. The Late Cenozoic Hurricane fault scarp forms the western boundary of the area, and uplift along this fault set up conditions that led to the erosional phenomena.
Laramide fault blocks and forced folds of the Livermore-Bellvue area, Colorado
Authors: Matthews Vincent 
Published: November 2007

Abstract
Location and Access. Four localities north of Fort Collins, Colorado (Fig. 1) display many of the structural features found throughout the Wyoming province of the Rocky Mountain Foreland. All of the localities can be viewed from public roads that are easily accessible to passenger cars or buses.
Significance of Locality. The northeastern flank of the Front Range displays several varieties of Laramide folds as well as critical relationships for demonstrating that the folds in the sedimentary rocks are forced folds resulting from differential uplift of faulted blocks of Precambrian basement. Within this smallarea are several beautifully exposed monoclines; differentially up-lifted blocks (both tilted and untilted) of Precambrian basement;and well-displayed asymmetrical anticlines, synclines, domes, andbasins. The area is also cut by a major lineament that separatestwo major structural styles in the Front Range and Denver Basin(Matthews, 1976). In this small area, one can see most of the crucial relationships which bear on the controversy over the nature and origin of Laramide deformation in the Rocky Mountain Foreland Province. The sites are described in more detail in Matthews and others (1976), Matthews and Sherman (1976), and Matthews and Work (1978).
Precambrian structure, metamorphic mineral zoning, and igneous rocks in the foothills east of Estes Park, Colorado
Authors: Hutchinson Robert M. , Braddock William A. 
Published: November 2007

Abstract
The area is located in the north-central part of Colorado and is readily accessible via U.S. 34, which roughly divides the area into north and south halves (Fig. 1). The eastern boundary of the area is 8 mi (9 km) west of Loveland, where U.S. 34 enters Big Thompson Canyon. Big Thompson power plant and Little Dam are at the immediate entrance to the canyon. Hard-bottomed dirt roads run north and south from the highway and afford ready access to the eleven stops shown on Figure 1)1.
Paleozoic-Mesozoic section
Authors: Weimer Robert J. , Roy L. W. Le 
Published: November 2007

Abstract
Several significant sections of Paleozoic and Mesozoic rocks occur in close proximity to one another at the foot of the Front Range west of Denver. The Paleozoic section on the east flank of the central Front Range is well exposed in Red Rocks Park. Excellent exposures of the Mesozoic section are at the 1-70 Road Cut, and along Rooney Road, east of the Dakota Hogbak on the southeast side of 1-70.
Location and access. Red Rocks Park is located northwest of Morrison, Colorado, 10 mi (16 km) west of Denver (Fig. 1). The 1-70 Road Cut is located west of Denver, 3 mi (5 km) south of Golden, Colorado, and is the point at which 1-70 cuts the Dakota Hogback. Rooney Road is east of the Dakota Hogback on the southeast side of 1-70. To reach all three sites, proceed west from Denver about 10 mi(16 km) on 1-70. Leave 1-70 at the Morrison Exit, which is well marked. A parking lot and footpath adjacent to the exit provide access to the 1-70 Road Cut site. To reach the Red Reeks and Rooney Road sites, proceed south from the exit on Colorado 26. About 1 mi (1.6 km) south of 1-70, signs at a marked intersection will direct one west to Red Rocks Park, or east to Rooney Road via Colorado 26 (Alameda Parkway). All three localities are on publicly owned lands and can be reached by passenger car. Adequate parking is available at each locality. Generalized lithologies and
The Florissant Fossil Beds National Monument, Teller County, Colorado
Authors: Hutchinson R. M. , Kolm K. E. 
Published: November 2007

Abstract
The Florissant National Monument is easily accessible by taking U.S. 24 west from Colorado Springs to the small town of Florissant, 35 mi (56 km) away (Fig. 1). At the town center, turn south toward Cripple Creek on the unpaved Teller County Road No. 1. The national monument is 0.5 mi (0.8 km) from the town of Florissant. The entire national monument area can be seen in half a day’s time.
The Garden of the Gods and basal Phanerozoic nonconformity in and near Colorado Springs, Colorado
Authors: Noblett Jeffrey B. , Cohen Andrew S. , Leonard Eric M. , Loeffler Bruce M. , Gevirtzman Debra A. 
Published: November 2007

Abstract
The Garden of the Gods, a city park within the Colorado Springs city limits, is located on the eastern flank of the Colorado Front Range (Fig. 1). It can be reached by following the Garden of the Gods Road (exit 146 from I-25) west 2.4 mi (3.8 km) until it curves to the south and becomes 30th Street. Continue south 1.5 mi (2.4 km) to an unnamed road marked by a small sign (Garden of the Gods) and turn right (west) into the park. Mesa Road, which veers uphill from 30th Street 0.8 mi (1.3 km) north of the turnoff to the park, crests at a spectacular overview of the park and surrounding areas. Several U.S. Geological Survey 7½-minute quadrangle maps cover this region. The Garden of the Gods lies mostly within the Pikeview and Cascade Quadrangles; with its southern part in the Colorado Springs and Manitou Springs Quadrangles. The two stops described here are all on public land and can be reached by passenger car.
Grenadier fault block, Coalbank to Molas Passes, southwest Colorado
Authors: Baars D. L. , Ellingson J. A. , Spoelhof R. W. 
Published: November 2007

Abstract
The Grenadier fault block is a paleotectonic complex exposed in the heart of the San Juan Mountains of southwestern Colorado. Structural and stratigraphic complexities are well exposed by the effects of Pleistocene glaciation and Recent erosion at and above timberline in a rugged alpine setting (Fig. 1). U.S 550 traverses the region between Durango and Silverton, affording excellent access. The most critical exposures lie within T.40N., R.7,8W., near the intersection of 37°45’N. and 107°45’ W. in LaPlata and San Juan Counties. Elevations range between 9,000 and 14,000 ft (3,300-5,133 m), effectively limiting field observations to mid-summer months. The area lies within the San Juan National Forest; access is therefore unrestricted. However, due to the rough terrain, appropriate safety precautions should be observed.
San Francisco Mountain
Authors: Helm Richard F. 
Published: November 2007

Abstract
San Francisco Mountain, about 6 mi (10 km) north of Flagstaff, Arizona (Fig. 1), is a composite volcano in the San Francisco volcanic field of northern Arizona; the volcano is situated on the southern Colorado Plateau about 31 mi (50 km) north of the escarpment that forms its topographic edge. Flagstaff, the major city in the volcanic field, is at the junction of 1-40, U.S. 180, and U.S. 89, the latter two highways passing San Francisco Mountain on its west and east sides, respectively. Access to the mountain is by unpaved U.S. Forest Service roads, most of which are passable by low-clearance vehicles; a few primitive roads require 4-wheel-drive vehicles.
A ski resort on the west side of the mountain normally operates its chairlift during the summer months, providing easy access to the 11,600 ft (3,512 m) level on Agassiz Peak. Hiking restrictions are in effect on Agassiz and Humphreys Peaks, and the designation of the upper part of San Francisco Mountain as the Kachina Peaks Wilderness Area imposes wilderness area restrictions. The Inner Basin is reached by foot or with a vehicle permit from the U.S. Forest Service. The Elden Ranger District office in Flagstaff should be consulted in planning a back-country trip.
Ship Rock, New Mexico
Authors: Delaney Paul T. 
Published: November 2007

Abstract
Ship Rock, the erosional remnant of an Oligocene volcanic vent, is a prominent feature of the skyline in northwest New Mexico. It rises 1,700 ft (500 m) above a surrounding plain, 24 mi (38 km) south-southeast of the Four Corners and 10 mi (17 km) southwest of the town of Shiprock.
Upper Cretaceous-Paleocene sequence, northwestern New Mexico
Authors: Kues Barry S. , Lucas Spencer G. 
Published: November 2007

Abstract
The area discussed here is in San Juan County, New Mexico, approximately 30 mi (48 km) south of Farmington and 20 mi(32 km) northwest of Chaco Canyon National Monument (Fig. 1). The small settlement of Bisti is most conveniently reached by traveling south on New Mexico 371 from Farmington or north on New Mexico 57 and New Mexico 371 from Thoreau, which is about 73 mi (117 km) east of Gallup on 1-40. Both of these routesare paved to within a few miles of Bisti. From New Mexico 44 atHuerfano an improved dirt road (County Road 15) runs southwest about 25 mi (40 km) to intersect New Mexico 371 about 9 mi (14 km) south of Bisti.
All of the stops indicated on Figure 1 are accessible by two-wheel drive vehicles, but many of the side roads into the badlands and arroyo areas require four-wheel drive. Viewing of areas off the main roads is best done on foot. The nearest gasoline, food, and water are in Farmington and several stores along New Mexico 44. Most of the area under consideration is within recently established federal wilderness areas, managed by the U.S. Bureau of Land Management (BLM). A few sections are owned by the State of New Mexico or the Navajo Nation, but no part of the area is within the Navajo Reservation. Permission is not required to examine exposures on federal or state land (a permit from the BLMis required to collect fossils), but permission should be obtained from the few
Precambrian-Upper Paleozoic geology along I-40 east of Albuquerque, New Mexico
Authors: Connolly James R. , Kues Barry S. 
Published: November 2007

Abstract
1–40 follows Tijeras Canyon through the Precambrian coreand overlying Pennsylvanian-Lower Permian sequence of the south end of the Sandia Mountains, beginning immediately eastof the Albuquerque city limits. Geologic features of this area are well displayed in road cuts and exposures near 1–40 and are summarized in this text for an 8.6-mi (13.8-km) interval of 1–40, beginning at the eastbound Carnuel (locally pronounced “carnway”) exit (Fig. 1). This section of 1–40 was constructed with wide shoulders, and there are numerous places where, with reasonable care, it is safe to stop along the highway to examine road cuts. Site descriptions, below, progress from west to east(from Precambrian to Permian), but the traveler should be aware that most of the road cuts referred to are on the north side of the interstate highway, along the west-bound lane. To examine them closely, if proceeding eastward, it is necessary to carefully cross the interstate or to drive to a nearby exit and backtrack. Short hikes off the highway, particularly in Precambrian terranes, can be most informative, and old U.S. 66, which parallels 1–40 between Carnuel and Tijeras, provides the safest access for a “hands-on” look at the Precambrian geology. Recent geologic maps of the area considered here were published by Kelley and Northrop (1975); Myers and McKay (1976) and Connolly (1982).
White Sands National Monument, New Mexico
Authors: LeMone David V. 
Published: November 2007

Abstract
White Sands National Monument is located in west-central Otero and east-central Dona Ana Counties in south-central New Mexico (Fig. 1). It is within and bounded by the White Sands Missile Range. The monument has a visitor’s center with the usual facilities. It is open year-round with the single exception of Christmas Day. Summer hours (Memorial Day to Labor Day) are from 8 A.M. to 10 P.M. Winter hours are from 8:30 A.M. to sunset. Periodic trips to Lake Lucero led by monument personnel are planned for every other month. These trips are subject to change depending on weather conditions and the firing schedule at White Sands Missile Range. Information concerning these special trips may be obtained by phoning (505) 437-1058.
Stratigraphy and sedimentology of the Paleocene Fort Union Formation along the Powder River, Montana and Wyoming
Authors: Flores Romeo M. 
Published: November 2007

Abstract
Extensive areas of the Powder River Basin in southeast Montana and northeast Wyoming are underlain by the Paleocene Fort Union Formation (Fig. 1). The sites selected for the field guide (Fig. 1) are easily accessible via the Powder River road from U.S. 212 (Broadus, Montana) to U.S. 14-16 (northeast of Arvada, Wyoming). The Powder River road is a county road that has a hard gravel surface easily traversed by cars. The outcrops are located either immediately along the road or only 0.25 mi (0.4 km) from the road. The lands along the Powder River are either managed by the Bureau of Land Management or privately owned by ranchers, who reserve the right to grant access to these lands. However, numerous field trips sponsored by the American Association of Petroleum Geologists, U.S. Geological Survey, North Dakota Geological Survey, and Casper College have been permitted access to the study sites. Permission was provided with the agreement that field-trip participants respect the land by not littering, not leaving gates open to stock, and carefully observing fire prevention rules. The rancher to contact for sites 1 and 2 is William Gaye, and the rancher for site 3 is Richard Reese. Mr Gaye maintains a ranch house on the Powder River road; Mr. Reese has a residence in the vicinity of Leiter, Wyoming (Fig. 1).
Southern Lemhi Range, east-central Idaho
Authors: Hait M. H. 
Published: November 2007

Abstract
The Lemhi Range, Idaho, is one of three northwest-trending basin-ranges along the northeastern margin of the eastern Snake River Plain (Fig. 1). The southern end of the range is about 55 mi (88 km) northwest of Idaho Falls. The small town of Howe is the closest location for food, water, gasoline, and a trailer park. The nearest motels and service stations are in Arco, about 22 mi(35 km) to the southwest. The area is covered by six 1:24,000 topographic quadrangles. They are listed in the caption of Figure 2A and will be essential for detailed planning of access.
Access to the outcrops is provided by graded dirt roads from Howe to the alluvial apron where rougher roads (traversable by pickups) lead to the seven major canyons in which the stratigraphic sections are exposed (Fig. 2A). From west to east, these canyons are South Creek Canyon, Black Canyon, Middle Canyon, East Canyon, Box Canyon (informal name), an unnamed canyon with a jeep road that crosses the range, and, on the east side of the range, Kyle Canyon.
Silurian Carbonate Mounds, Palisades-Kepler State Park, Iowa
Authors: Witzke Brian J. 
Published: November 2007

Abstract
Silurian strata are exposed at numerous localities ineast-central and northeast Iowa (Fig. 1), where the total Siluriansequence approaches 500 ft (150 m) in thickness. The bulk of thesequence is dominated by dolomite and cherty dolomite characteristically lacking a notable siliciclastic component. The Siluriancarbonates are pervasively dolomitized, except along portions of the northern and northwestern margins of the outcrop belt, where limestones occur. The Silurian early Llandoverian-Ludlovian)dolomite sequence is divided into six formations (Bunker and others, 1985), and a variety of fossil associations characterize the Silurian sequence (Witzke, 1983).
The youngest Silurian rocks in Iowa are exposed in the southern region of the outcrop belt (Fig. 1) and are assigned, in ascending order, to the Scotch Grove and Gower formations. Strata encompassing a part of the Scotch Grove-Gower intervalare well exposed and publicly accessible in the valley of the Cedar River in and around the area of Palisades-Kepler State Park (Fig. 1, about 10 mi (16 km) southeast of downtown Cedar Rapidsand 4 mi (6.5 km) west of Mt. Vernon. The Cedar River has cutthrough Silurian carbonate mound and intermound facies in the area, displaying a series of exposures along forested slopes andbold cliffs, in part overhanging, that form the scenic palisades. The cliffs reach heights to 65 ft (20 m) in places. Hiking trails in the state park provide access to many of the exposures. The most spectacular and instructive exposures encompass localities Athrough F Fig. 1.
The
Cedar Valley Formation of the Coralville Lake area, Iowa
Authors: Bunker Bill J. , Witzke Brian J. 
Published: November 2007

Abstract
Coralville Lake (Fig. 1) was authorized under the Flood Control Act of 1938 as a means of moderating stream flow on the Iowa River. Construction of the dam was begun in 1949, thendelayed by the Korean conflict, and consequently not completed until 1958. Coralville Dam regulates runoff from 3,084 mi2(8,018 km2) of land upstream, providing flood protection to 1,703 mi2 (4,428 km2) of the Iowa River Valley below the dam. The U.S. Army Corps of Engineers maintains Coralville Lake asa multiple-use project providing primary benefits in flood control and low-flow augmentation, and secondary benefits in recreation, fish and wildlife management, forest management, and waterquality improvement. Lake MacBride (Fig. 1) is a subimpoundment of Coralville Lake. The lake and surrounding land compriseLake MacBride State Park, which is managed by he Iowa Conservation Commission.
Exposures along the valley walls of that portion of the IowaRiver which comprises Coralville Lake, afford one the opportunity to examine at numerous points along its extent the upper most portion of the Wapsipinicon Formation and the entire Cedar Valley Formation. Excellent exposures of the Coralville Member of the Cedar Valley Formation can also be seen in the valley walls of the Iowa River in Iowa City (Witzke, 1984a).
Pennsylvanian cyclothem near Winterset, Iowa
Authors: Heckel Philip H. 
Published: November 2007

Abstract
This section is located on the west side of U.S. 169 about 1.7 mi (2.7 km) south of its junction with Iowa 92 on the western outskirts of Winterset (Fig. 1; E line NE¼SW¼Sec.11, T.75N., R.28W., Madison County, Iowa). Because traffic on this highway can be heavy, pull well off onto the shoulder, and please do notcross the highway.