bluuebunny/crossref_metadata_2025_split huggingface dataset:
Cache Creek-Ashcroft area, western Intermontane Belt, British Columbia
Authors: Travers William B. 
Published: November 2007

Abstract
Outcrops in and near the settlements of Cache Creek and Ashcroft, southern British Columbia (Fig. 1), provide an opportunity to view some of the structures and rocks that help to explain the evolution and amalgamation of the allochthonous terranes of the southern Canadian Cordillera. Sediments and igneous rocks ofthe Cache Creek and Nicola Groups formed in late Paleozoic to late Triassic times in oceanic and island arc settings. The sediments of the Ashcroft Formation were deposited from Early through Middle Jurassic time in an arc-related basin. In Late Jurassic or possibly earliest Cretaceus time, thrust faulting juxtapose Cache Creek-Nicola rocks over Ashcroft strata. This event is thought to have sutured these terranes to Quesnellia of which the Ashcroft Formation is generally considered to be a part. This faulting may havebeen related to the early (Late Jurassic) deformationin the Omineca Crystalline Belt when east-directed thrust faults joined Quesnellia to that crystalline terrane.
Sedimentology of the Upper Cretaceus Nanaimo Basin, British Columbia
Authors: Pacht Jory A. 
Published: November 2007

Abstract
The Nanaimo Group is an assemblage of conglomerate, sandstone, siltstone, shale, and minor coal deposited in the Nanaimo Basin during Santonian through Maestrichtian time (Muller and Jeletzky, 1970; Ward, 1978). It crops out on southeastern Vancouver Island, the Gulf Islands of British Columbia, and the San Juan Islands of Washington (Figs. 1, 2). Nearly continuous outcrops of the Namaimo Group occur along seacliffs on Vancouver Island, and on the Gulf and San Juan islands. Good exposures are also present along roadcuts and major rivers on Vancouver Island.
Ferries from the mainland to Vancouver Island and most of the Gulf and San Juan islands can be boarded at Anacortes, Washington, and Tawassen, British Columbia, and taken to Sidney, British Columbia (approximately 20 mi, 32 km, north of Victoria on Vancouver Island), and to the San Juan and Gulf islands, respectively. Ferries can also be taken from Port Angeles, Washington, to Victoria, British Columbia. In addition, ferries run regularly between islands in both Canada and Washington. Current ferry schedules are necessary for travel in this area.
Tidelands are considered public property in both Canada and the United States; access to the outcrops is available at many public beaches.
The Cenozoic section at Suntrana, Alaska
Authors: Wahrhaftig Clyde 
Published: November 2007

Abstract
The Cenozoic section at Suntrana in the Nenana coal field is located at Lat.63°52’N, Long.148°51’W, Healy D-4 Quadrangle, 3 to 3.5 mi (5 to 6 km) east of the Nenana River, on the north bank of Healy Creek and on Suntrana Creek, its 1.2-mi-long (2 km) tributary at this point (Figs. 1 and 2). It is approximately 6.7 mi (10.8 km) east, by automobile road, of mile 248.8 (km 400.4) on the George Parks Highway. Mile 248.8 is 7 mi (11.5 km) north on the highway from the entrance to Denali National Park. Suntrana Creek is narrow and shallow and is easily crossed dryshod most of the year. Its upper 1 mi (1.5 km) is usually dry. Vehicles should not be parked close to the crossing of Suntrana Creek, and one should not be in its canyon whenever storms are imminent, for during heavy rains masses of mud and water as much as 25 ft (8 m) deep have come raging down the creek.
Delta River area, Alaska Range, Alaska
Authors: Péwé Troy L. 
Published: November 2007

Abstract
The Alaska Range is a glacially sculptured, arcuate mountain wall extending west and southwest 600 mi (1,000 km) in central Alaska from the Canadian border to the Aleutian Range. It is extremely rugged and includes Mt. McKinley (20,443 ft; 6,195 m elevation), the highest mountain on the North American continent. The Delta River, 75 mi (125 km) long, originates on the south side of the range in the Tangle Lakes and flows northward through the range to the Tanana River. The Richard-son Highway (Fig, 1) crosses the range through the Delta River valley, which is 0.6 to 12 mi (1 to 20 km) wide and 60 mi (100 km) long. Because of the lack of villages, cities, and towns, references to geographical points in the valley have been referenced to mile posts on the Richardson Highway since the early part of this century. This practice will be continued in this report. Mile O on the highway is at Valdez, a town on the Gulf of Alaska and the terminus of the Trans-Alaska Pipeline System; the highway ends at mile Fairbanks 363.8.
Landslide and debris-flow deposits in the Thumb Member of the Miocene Horse Spring Formation on the east side of Frenchman Mountain, Nevada
Authors: Salyards Stephen L. , Shoemaker Eugene M. 
Published: November 2007

Abstract
From the south: From Henderson, Nevada, take Lake Mead Drive (Nevada 147). At 7.1 mi (11.4 km) east of U.S. 95, turn north onto Northshore Road and go 3.2 mi (5.1 km) to Lake Mead Boulevard. The site is 3.7 mi (6 km) north on Lake Mead Boulevard.
From the north: From North Las Vegas, take Lake Mead Boulevard (also Nevada 147) east from 1–15. At 11.4 mi (18.3 km) from 1–15 a paved road from the east (left) intersects Nevada 147. Continue on 147 for 1.8 mi (2.9 km) to the site.
The site is marked by the high-tension power line that crosses the road. Park along the side of the road or on the dirt roads that intersect the main road in this area.
Coastal and volcanic geology of the Hanauma Bay area, Oahu, Hawaii
Authors: Moberly Ralph , Walker George P. L. 
Published: November 2007

Abstract
The Hanauma Bay-Koko Fissure area occupies the southeastern tip of the island of Oahu, Hawaii (Fig. 1), and is shown on the Koko Head 71/2-minute Quadrangle. The Geologic Map of Oahu (1:62,500; Stearns, 1939) is out of print. A 1:500,000 colored geologic map of the state and generalized chart shows the Honolulu and Koolau volcanic groups-relative to other rock units (Bennison, 1974).
Access is easy by automobile. Buses of No. 1 route, marked “Lunalilo Home Road,” give frequent service from Honolulu to the Lunalilo Home Road point described below as mileage point zero. Buses of No. 58 route travel from Waikiki to that point. Traffic on the winding, narrow highway between stops 2 and 4 demands caution as does high surf on the seacliff. The area is within a park offering generally free access.
The Keystone and Red Spring thrust faults in the La Madre Mountain area, eastern Spring Mountains, Nevada
Authors: Axen Gary J. 
Published: November 2007

Abstract
The La Madre Mountain area lies about 9 mi (15 km) west of Las Vegas, Nevada (Fig. 1). Access is provided to sites 1 through 5 by side roads off of West Charleston Boulevard, and site 6 is reached from U.S. 95 northwest of town. The sites are meant to be visited in consecutive order, and the mileages given begin at the I-15 and West Charleston exit. Although the first fivesites are accessible by any vehicle, site 6 may necessitate a vehicle with a high center. Four-wheel drive is not necessary.
U.S. Geological Survey topographic maps for the area are the La Madre Mountain and Blue Diamond NE 7½-minute Quadrangles. Site 4 is on the easternmost edge of the Mountain Springs 15-minute Quadrangle.
Fault scarps formed during the earthquakes of October 2, 1915, Pleasant Valley, Nevada
Authors: Wallace Robert E. 
Published: November 2007

Abstract
Four fault scarps that formed during the earthquakes of October 2, 1915, are located in north-central Nevada, 150 mi (240 km) northeast of Reno, and 30 to 55 mi (48 to 88 km) south of Winnemucca (Fig. 1). A site along the largest of the four scarps, the Pearce scarp, at Golconda Canyon on the west flank of the Tobin Range (Sec. 5, T28N, R.39E, Mt. Tobin 15-minute Quadrangle) is easily reached by driving south about 45 mi (72 km) from Winnemucca along the Grass Valley-Pleasant Valley road, which is paved for about 7 mi (11.2 km) after which it is graded gravel. At the Golconda Canyon road, go east 1.5 mi (2.4 km) to the fault scarp at the range front. The Pearce scarp is also clearly visible from the Pleasant Valley road for about 15 mi (24 km) and excellent photo sites abound. Afternoon lighting emphasizes the scarp especially well. The Sou Hills scarp (3–6 ft) (l-2 m) high, can be seen in the distance to the south from near the junction of the Pleasant Valley-Dixie Valley roads. Additional map coverage is provided by the Cain Mountain and Fencemaker 15-minute and the China Mountain 71/2-minute Topographic Maps.
Lamoille Canyon nappe in the Ruby Mountains metamorphic core complex, Nevada
Authors: Howard Keith A. 
Published: November 2007

Abstarct
The Ruby Mountains form a high and rugged range in northeastern Nevada. Lamoille Canyon in the Ruby Mountains is an easy half-hour drive by passenger car from the town of Elko (Fig. 1). From Elko, located on 1–80, take Nevada 227 southeast for 19 mi (30 km) to a sign marking a right turn onto the Lamoille Canyon road. This paved road leads south into the Ruby Mountains and ascends Lamoille Canyon for 10 mi (16 km) to an elevation of 8,730 ft (2,661 m). The site is best visited in summer, for the canyon is generally snowbound from November to May. The Lamoille Canyon road offers spectacular mountain scenery and a U.S. Forest Service campground. Geologic features are well exposed in roadside outcrops and in glaciated canyon walls 2,000 to 4,000 ft (600 to 1,200 m) high. To enhance your visit, bring a camera, a geologic road log (Snoke and Howard, 1984), a colored 1:125,000-scale geologic map (Howard and others, 1979), and the Lamoille, Nevada, 15-minute topographic quadrangle published by the U.S. Geological Survey.
Island Park, Idaho; Transition from rhyolites of the Yellowstone Plateau to basalts of the Snake River Plain
Authors: Christiansen Robert L. , Embree Glenn F. 
Published: November 2007

Abstract
Island Park, situated between the northeastern end of the Snake River Plain and the western margin of the Yellowstone Plateau, is traversed by U.S. 20-191 between Ashton, Idaho, and West Yellowstone, Montana (Fig. 1) and, in part, by the Mesa Falls Road (Idaho 47). All of the physiographic and geologic features described in this guide can be reached during the summer months by passenger car on those two paved highways or on short gravel roads that extend from them. During the winter, U.S. 20-191 remains open, but other winter travel is possible only by skis or skimobile. One quarry locality described later is privately owned but has generally been freely accessible.
A Neogene(?) gravity-slide block and associated slide phenomena in Swan Valley graben, Wyoming and Idaho
Authors: Moore David W. , Oriel Steven S. , Mabey Don R. 
Published: November 2007

Abstract
The gravity-slide block lies below the steep west flank of the Snake River Range near Alpine, Wyoming. Alpine is 37 mi (60 km) southwest of Jackson, Wyoming, via U.S. 89-26 and 73mi (117 km) east of Idaho Falls, Idaho, via U.S. 26. A Forest Service campground and several motels, restaurants, and stores are located at Alpine.
Rocks are well exposed at three stops on U.S. 26 north of Alpine along the east shore of Palisades Reservoir (Fig. 1). All stops are in the Targhee National Forest. No permission is required to visit them and all are accessible by passenger car when roads are dry. Stop 2 is reached by hiking 0.4 mi (0.7 km) overland and climbing 650 ft (200 m).
Stop 1 is in Long Springs Canyon (SW¼NW¼Sec.17,T.37N.,R.118W. on the Alpine Quadrangle map; Albee and Cullins, 1975). Drive 1.9 mi (3 km) north on U.S. 26 from the junction of U.S. 26 and 89 to a gravel road at the U.S. Forest Service sign“4-H Camp.” Turn east into Targhee National Forest and go 1.0 mi (1.6 km). Drive through the 4-H Camp and Idaho State University Geology Field Camp and across Long Springs Creek. An optional stop 1A is 0.2 mi (0.3 km) east and 0.2 mi (0.3 km) north.
Stop 2 is reached via an unimproved dirt road that is 1.3 mi (2.1 km) north of the 4-H Camp road intersection on U.S. 26. Drive east 0.5 mi (0.8 km) to the end of the dirt road. Walk upslope through the woods north-northeast to the base of the tan cliffs
Geology of the Craters of the Moon lava field, Idaho
Authors: Kuntz Mel A. , Champion Duane E. , Lefebvre Richard H. 
Published: November 2007

Abstract
The most convenient place to see the Craters of the Moon (COM) lava field is at Craters of the Moon National Monument, reached by U.S. 20-26 from either Arco or Carey, Idaho (Fig. 1). A 7-mi (11-km) loop road and several hiking trails provide accessto volcanic features within the Monument Fig. 2. The 20-mi long (32-km) Wilderness Trail is the longest of the trails and requires a permit for overnight trips; there is no potable water available along this trail. The east, south, and west edges of the COM lava field can be reached by four-wheel-drive vehicles on unimproved roads that are shown on U.S. Geological Survey 7½-minute quadrangle maps of the area. The geologie map of the Inferno Cone Quadrangle (Kuntz and others, 1986c) depicts the volcanic features that are most accessible to visitors to the monument. Please note that hammers may not be used and samples may not be taken in the monument.
The Montini Volcano; A lava dam on the ancestral Snake River, southwest Idaho
Authors: Malde Harold E. 
Published: November 2007

Abstract
The name Montini Volcano is applied to a much-dissected basaltic vent where Sinker Creek joins the canyon of the Snake River southwest of Boise Fig. (1). The name comes from Montini Ranch—now the Nahas Ranch—on the 1949 edition of the Sinker Butte Topographic Quadrangle (1:24,000). The Volcano is also partly with in the adjacent Wild Horse Butte Quadrangle. Downcutting by the Snake River and Sinker Creek has exposed the plug of the volcano and nearly 600 ft (180 m) of its surrounding tuff and lava.
The Montini Volcano can be reached from milepost 33 on Idaho 78 by following the road shown in Figure 1. Just before reaching Sinker Creek, a single-lane track negotiable by passenger cars leads down Sinker Creek to the central plug of the volcano Fig. (2). Although a gate has been installed at the head of the track to control livestock, the track is open to the public. From the plug, the track continues to a pumping station one mi (1.6 km) down the Snake River (NW¼Sec.6,T.3S.,R.l E.). From here, looking upstream, one has a splendid view of the dissected volcano (Fig. 3). Those wanting to see other parts of the Montin Volcano must back track to the Nahas Ranch and ask permission to use the ranch road. From the ranch headquarters, this roadleads southeast and then northeast to a point on the Snake River about 2 mi (3 km) above the mouth of Sinker Creek. A single lane track on the north
The Late Proterozoic Pocatello Formation; A record of continental rifting and glacial marine sedimentation, Portneuf Narrows, southeastern Idaho
Authors: Link Paul Karl 
Published: November 2007

Abstract
Portneuf Narrows is located on the Inkom, Idaho, 1:24,000 Topographic Quadrangle. The area is ideal for a one-day field trip because it is accessible from 1–15 (Exit 63-Portneuf Area) and is only 3 mi (4.8 km) from Pocatello where tourist services and the Idaho State University Library are available. Stops 1 and 3 are on paved roads. Stop 2 is on a dirt road that can be driven by passenger cars in dry weather. The entire area is on public land.
Stop 1 is an overview of Portneuf Narrows (Fig. 1A); it is reached by heading southeast from Pocatello on I–15 and taking exit 63S. Turn west (right) onto the frontage road (South Fifth Avenue), proceed 0.7 mi (1.1 km), cross under the freeway, and stop on the east side of the frontage road. If approaching from the south (Salt Lake City), take exit 63N, turn right at the frontage road, and proceed 0.2 mi (0.3 km) to Stop 1 on the left side of the road.
The outcrops south of Portneuf Narrows (Stop 2) are reached by heading south on Fort Hall Mine Road from exit 63. Cross the Union Pacific Railroad and the Portneuf River and proceed 0.2 mi (0.3 km) to Portneuf Road. Cross it, and continue straight for 0.6 mi (l km). There, bear left onto dirt road (avoiding road to sanitary landfill) and park at locked gate in Fort Hall Mine Canyon (Stop 2, Fig. 1A). The most complete stratigraphic sections can been seen in the base of the second canyon
Heart Mountain detachment fault and elastic dikes offault breccia, and Heart Mountain break-away fault, Wyoming and Montana
Authors: Pierce William G. 
Published: November 2007

Abstract
This text includes two sites: the first is the Heart Mountain detachment fault and elastic dikes of fault breccia (Site 33 in Fig. 1); the second, located 1 mi (2 km)to the west of the first, is a related feature termed the Heart Mountain break-away fault (Site 33 in Fig. 1). If only one site can be examined, Site 33 should be selected: It is more accessible, and has better exposures and more features pertaining to the Heart Mountain fault.
Site 33 (Fig. 1), showing the Heart Mountain detachment fault and elastic dikes, is situated 0.5 mi (0.8 km) due south of Silver Gate, Montana. It can be reached on foot by climbing a steep mountain slope (600-vertical ft (180-m) gain in 1,800 ft (540 m), beginning at the end of the road 1,000 ft (300 m) south of the Post Office. The site is on public land but at the outset 300 ft (100 m) of private land must be crossed when taking the most direct route. The owner of the undeveloped private land does not object to scientists crossing her land to reach Site 33.
Rhyolite-basalt volcanism of the Yellowstone Plateau and hydrothermal activity of Yellowstone National Park, Wyoming
Authors: Christiansen Robert L. , Hutchinson Roderick A. 
Published: November 2007

Abstract
A volcanic plateau constructed by late Pliocene and Quaternary eruptions spans the Continental Divide and occupies the central part of Yellowstone National Park, mainly in northwestern Wyoming but overlapping into eastern Idaho and southwestern Montana. The National Park is accessible by road through five entrances, reached by U.S. 20 from the west and east, from the north and south, and U.S. 212 from the northeast (Fig. 1). The localities described in this guide are all on or adjacent to the park road system and can be reached, during the summer months (usually early May through late October), by passenger car or, during the winter, by skis or skimobile. A nominal entry fee for vehicles is valid in both Yellowstone and Grand Teton national parks.
Special caution should be exercised in visiting the thermal 89 areas; they are both delicate and dangerous. Designated walk-ways are provided in the thermal areas described here, and posted park regulations should be followed. Specimen collecting in the national park is allowed only by permit, which can be issued by the National Park Service only in advance of a collecting trip.
Idaho- Wyoming thrust belt
Authors: Ore H. Thomas , Kopania A. A. 
Published: November 2007

Abstract
This guide describes two areas of observation in the Idaho-Wyoming thrust belt. The first is a 3-mi (4.9-km) long section on Teton Pass, west of Jackson, Wyoming, along Wyoming 22 (Fig. 1). The geologic map (Fig. 2) and discussion below refer to a section that stretches from 2.5 mi (4.0 km) west of the summit of Teton Pass to 0.5 mi (8.0 km) to the east. The area is depicted on the Teton Pass and Rendezvous Peak 7¼-minute Geologic Quadrangle Maps (Schroeder, 1974, 1976). The second area is along the Hoback Valley and Canyon, about 10 mi (16 km) southeast of Jackson. Observations there are along U.S. 187–189, from Hoback Junction to Granite Creek, about 11.5 mi (18.5 km) east. The area is depicted on the Camp Davis and Bull Creek 7¼-minute Geologic Quadrangles (Schroeder, 1974, 1976). Two other locations in the area are briefly described. They are both on U.S. 26–89 in the Grand Canyon on the Snake River. The first is about 3 mi (4.8 km) southwest of Hoback Junction, where the Darby thrust is exposed, the other is at Keyser Creek, about 8 mi (12.9 km) east of Alpine Junction, where the Little Greys Anticline is exposed. All locations described herein are on public land.
Hoback River Canyon, central western Wyoming
Authors: Dorr John A. , Spearing Darwin R. , Steidtmann James R. , Wiltschko David V. , Craddock John P. 
Published: November 2007

Abstract
Geologic features along the Hoback River Canyon in central western Wyoming illustrate tectonic effects and stratigraphic and structural evidence for dating thrusts and later listric normal faults in part of the Idaho-Wyoming Thrust Belt and adjacent Foreland. Figure 1 and Table 1 combine to show that major thrusts in the Thrust Belt young in thedirection of tectonic transport, in this case from west to east, the oldest being the Paris Thrust and the youngest the Prospect. The preeminent features, logged below and visible from the highway (Fig. 2) are, west to east, the Hoback Fault (listric normal), Bear Thrust, Prospect (=Cliff Creek=Jackson) Thrust and Game Hill Thrust. These are capitalized on Table 1.
The site description begins on the west at Hoback Junction, 13 mi (21 Km) south of Jackson, Wyoming, on U.S. 187-189. It follows U.S. 187-189 east from there for 16 mi (26 km) with four stops enroute (Fig. 2). It crosses from south-central Teton County into northwestern Sublette County within U.S. Geological Survey Camp Davis and Bull Creek 7½-minute tomographic and geologic map quadrangles. Small-scale colored geologic map and cross-section sheets, which include the site, are in the pocket at the back of Dorr and others, 1977. A detailed road log of this area is given by Spearing and Steidtmann (1977).
Sandstones of the Casper Formation of the southern Laramie Basin, Wyoming
Authors: Steidtmann James R. 
Published: November 2007

Abstract
Very large scale, trough cross-stratification in sandstone units of the Casper Formation is well exposed along Sand Creek in the southernmost Laramie Basin, Wyoming (Fig. 1). The exposures of features described herein are located in the SW¼, Sec.31, T.13N., R.74W. and the E½, Sec.l, T.12N., R.75W.(Fig. 1). This locality is included in a field trip guide by Steidtmann and Weimer (1976); photographs of the features mentioned herein are in Steidtmann (1974, 1976).
Early Proterozoic and Precambrian-Cambrian unconformities of the Nemo area, Black Hills, South Dakota
Authors: Redden Jack A. 
Published: November 2007

Abstract
Excellent exposures of both an early Proterozoic uncon formity and the Precambrian-Cambrian unconformity occur in the Nemo area along the eastern side of the Precambrian core of the Black Hills approximately 18 mi (30 km) northwest of Rapid City (Fig. 1). Although the two unconformities are exposed relatively near one another, there is approximately 1.5 Ga difference in their ages. The lithologies and structure of these localities permit significant inferences about tectonic events and geologic history of the Black Hills.
Harney Peak Granite and associated pegmatites, Black Hills, South Dakota
Authors: Shearer C. K. , Papike J. J. 
Published: November 2007

Abstract
The Harney Peak Granite is located in the south-central portion of the Precambrian core of the Black Hills, South Dakota. This field study includes five sites near Keystone, South Dakota (Figs. 1 and 2). All sites are accessible by passenger car. At Site 1, the Harney Peak Granite is exposed at the Mount Rushmore National Memorial. (Large groups visiting at Mount Rushmore are expected to check in at the memorial headquarters.) Hammers or sample collecting are not allowed at the Rushmore site. A suite of Harney Peak Granite maybe collected to the west of the memorial (Site la). Sites 2 through 5 are pegmatites (Diamond Mica, Etta, Peerless, and Dan Patch) associated with the Harney Peak Granite. Permission for access to the Etta pegmatite may be obtained from the Pacer Corporation, Box 912, Custer, South Dakota 57730 (605/673-4458). Permission for access to the Peerless pegmatite maybe obtained from the Rushmore Borglum Museum in Keystone, South Dakota (605/666-4449). The other sites are on public land.