bluuebunny/crossref_metadata_2025_split huggingface dataset:
Geologic framework of the Boise Warm Springs geothermal area, Idaho
Authors: Wood Spencer H. , Burnham Willis L. 
Published: November 2007

Abstract
The Boise Warm Springs area is 2 mi (3.3 km) southeast of the Idaho State Capitol building (Fig. 1). Turn north from Warm Springs Avenue onto Old Penitentiary Road. Take the first left turn, about 200 ft (70 m), and proceed west about one block to Quarry View City Park. A major part of the area is a public park administered by the City of Boise and the Idaho Historical Society. A prominent outcrop of rhyolite, locally known as “Castle Rock” is on private land, but at the present time access is not restricted.
Thousand Springs area near Hagerman, Idaho
Authors: Whitehead R. L. , Covington H. R. 
Published: November 2007

Abstract
Numerous spectacular springs discharge from the Snake Plain aquifer along the north side of the Snake River canyon near Hagerman, Idaho (Fig. 1). This stretch of canyon, known as the Thousand Springs area, contains 11 of the 65 springs in the United States that discharge more than 72,400 acre-ft annually (Meinzer, 1927, p. 27). The springs can be reached by automobile or can be viewed from a distance. Most springs are on private land and permission is needed to enter the area, but some, such as Niagara Springs, are on public lands.
Shoshone Falls, Idaho; A Pleistocene relic of the catastrophic Bonneville Flood
Authors: Malde Harold E. 
Published: November 2007

Abstract
Shoshone Falls is on the Snake River about 4 mi (6 km) northeast of the city of Twin Falls, near the midpoint of a chaotically eroded 14-mi (22-km) section of the Snake River canyon (Fig. 1). The south side of the falls, where the city maintains apicnic ground and park, offers the best views. Westbound travelers on I–84 should take the Kimberly-Twin Falls exit (no. 182), cross the Snake River on the Hansen Bridge, drive 5 mi (8 km) west on Addison Avenue, and then follow the signs northward to the falls. Those traveling east should take the Twin Falls exit at U.S. 93 (no. 173), cross the Snake River on the Perrine Memorial Bridge, and drive 3 mi (5 km) east on Falls Avenue to the Shoshone Falls road. Viewpoints on the south rim of the canyon at both bridges are convenient stopping places to see the narrow canyon above the falls and the wide canyon enlarged by flood erosion downstream. The north side of the falls can be reached by an improved road leading from U.S. 93.
Evidence for the spillover of Lake Bonneville, southeastern Idaho
Authors: Bright Robert C. , Ore H. Thomas 
Published: November 2007

Abstract
The area described herein is in southeastern Idaho, in Franklin and Bannock counties. It is readily reached via I–15 and various paved state highways from any direction.
Each stop is easily accessible by two-wheel drive vehicles when roads are dry. However, the dirt roads leading to stops 1 to 6 can be extremely slick when soaked. Permission from property owners is required if you desire to wander beyond each stop.
The tour is keyed to the following 7½-minute quadrangles: Pocatello North, Inkom, Arimo, McCammon, Bonneville Peak, Downey West, Downey East, Oxford, and Swan Lake. The latter two are particularly important for locating features south of the overflow site. The Preston and Pocatello 2-degree quadrangles are also suggested.
The trip will take about six hours. It begins in northern Cache Valley at the hamlet of Oxford, proceeds northward through Red Rock Pass and Marsh Valley, and ends in the Pocatello area (Fig. 1). Food and lodging can be found in Preston (dry) and Pocatello.
Geology and evolution of the Grand Canyon of the Yellowstone, Yellowstone National Park, Wyoming
Authors: Richmond Gerald M. 
Published: November 2007

Abstract
The Grand Canyon of the Yellowstone is in east-central Yellowstone National Park. It is accessible from Canyon Village (Fig. 1, inset), where all facilities are available. Check in at the visitor center.
Observe park regulations stay on established trails unless you have off-trail permission; do not break rocks or hot-spring deposits; take no samples, not even loose pieces (collecting is not permitted); leave hammers, picks, and shovels in your vehicle. Suggested time: one full day.
The Rhodes allochthon of the Enos Creek-Owl Creek Debris-Avalanche, northwestern Wyoming
Authors: Bown Thomas M. , Love J. David 
Published: November 2007

Abstract
SE¼SE¼NE¼SW¼ Sec.17, NE¼NE¼SE¼SW¼ Sec.17, W¾N½SW¼SE¼ Sec.17, and W¾S½NW¼SE¼ Sec. 17, T.44N., R.99W., Hot Springs County, Wyoming (Fig. 1; Bown, 1982a, PI. 1). Twentyone Creek, Wyoming, Quadrangle (U.S. Geological Survey 7½ minute topographic series, 1956).
Zone of interaction between Laurentide and Rocky Mountain glaciers east of Waterton-Glacier Park, northwestern Montana and south western Alberta
Authors: Karlstrom Eric T. 
Published: November 2007

Abstract
The evidence for interaction between Laurentide and Rocky Mountain glaciers east of Waterton-Glacier Park can best be studied by examining a number of sites in the zone of glacier overlap and possible confluence. The 10 stops described in this field guide are located in the Saint Mary, Belly, and Waterton drainages in Montana and Alberta (Fig. 1). With the exceptions of Stops 1 and 10, which occur on the Blackfeet Indin Reservation and in Waterton Park, respectively, all stops occur on public roads through private land. Landowner’s permission is not required for the excursion as described but should be obtaine before collecting samples or extensive off-route exploration. The trip can be completed in a long half day with two-wheel drive vehicle. Those with less time may limit their trip to Stops 1 through 5 on the U.S. side or the approximately equivalent Stops 6 through 10 in Canada. The U.S. portion of the trip is covered by the Cutbank 1:250,000 topographic sheet and the Saint Mary, Babb, Duck Lake, Wetzel, Hall Coulee, Emigrant Gap, and Pike Lake 1:24,000 sheets. The Canadian portion is covered by the Lethbridge 1:250,000 sheet and the Cardston and Waterton Lakes (82 H/3 and H/4) 1:50,000 sheets.
Wind River Canyon, Wyoming
Authors: Maughan Edwin K. 
Published: November 2007

Abstract
The Wind River Canyon transects the Owl Creek Mountains near the center of Wyoming. The canyon is in the northwest quadrant of the state (Fig. 1) and within the northeast corner of the Wind River Indian Reservation. U.S. 20 traverses the canyon from a point about 15 mi (24 km) north of the town of Shoshoni in the Wind River Basin to the mouth of the canyon about 5 mi (8 km) south of Thermopolis in the Bighorn Basin. The Wyoming Geological Association and the State Highway Department have erected signs that label the geological formations within the canyon; many of the features that will be noted are referenced to mileposts along the highway.
Type Pinedale Till in the Fremont Lake area, Wind River Range, Wyoming
Authors: Richmond Gerald M. 
Published: November 2007

Abstract
The Fremont Lake area is at the southwest base of the Wind River Range, northeast of the town of Pinedale in Sublette County, Wyoming, (Fig. 1). It is included in the Fremont Lake South Quadrangle (scale 1:24,000) for which a topographic map, a geologic map (Richmond, 1973), and a soils map (Sorenson, 1986) are available.
The area is accessible from Pinedale on U.S. 191, about 100 mi (160 km) north of Rock Springs and 70 mi (112 km) southeast of Jackson. County Road 23-111 (paved) leads northeast from Pinedale into the area. Most of the terrain is in Bridger National Forest, but some is private land. All maintained roads are accessible by passenger car. Many unimproved roads require four-wheel drive. Obtain permission to enter gated roads. Respect signs; close all gates unless found open; and do not drive into areas under irrigation.
For a short tour, take County Road 23-11 f from the east end of Main Street in Pinedale toward Fremont Lake. The road leads up a terrace front, passes a cemetery, and extends northeast across gently rolling Bull Lake end moraines to an S-curve 2.2 mi (3.5 km) from U.S. 191. Here, the road ascends the steep, very bouldery front of the outermost Pinedale end moraine. Park at the bottom and walk 50 yd (46 m) up the road to a cut where Pinedale Till is well exposed (locality A, Fig. 1). Drive on to the moraine crest, from which an out standing overview of Fremont Lake, the enclosing Pinedale
Tertiary subsurface solution versus Paleozoic karst solution, Guernsey, Wyoming
Authors: Bridges L.W. (Dan) 
Published: November 2007

Abstract
Guernsey is located in southeastern Wyoming on the Hartville Uplift between Torrington and Douglas on U.S. 26.Guernsey State Park, which is 1 mi (1.6 km) north of U.S. 26, has an average elevation of 4500 ft (1400 m). It is readily accessible by car or bus anytime of the year because this is one of the warmest parts of Wyoming. Most of the outcrops are located in Guernsey State Park, which is in the Guernsey Reservoir quadrangle, Platte County, Sec.4, T.27N., R.66W., approximately 42°17'N,104°46'W.
Key locations to examine the problem of the nature of the solution surface on the top of the Guernsey Limestone are shown on Figure 1. An excellent view of the principal locality (B) (Fig. 2) on the east side of the North Platte River can be obtained from area A on the west side. The paleo-sinkhole at the south end of the exposure, and the solution surface to the north can be reached for closer examination by means of arduous hikes from parking lot C.
To reach the sinkhole area, walk southeasterly from the parking lot on the maintenance road, through the maintenance yards, down into a tributary valley and south along the river.
To see several 3 to 5 ft (1 to 1.5 m) solution arches, and a chert breccia (Fig. 3), on the solution surface, walk from the parking lot down to the top of the Guernsey Limestone and southward along this unconformity. Hiking here should be done with care because
Dunes of the Wyoming Wind Corridor, southern Wyoming
Authors: Marrs Ronald W. , Kolm Kenneth E. , Gaylord David R. 
Published: November 2007

Abstract
This geological field site, notorious for strong, persistent, unidirectional winds that have created classic eolian landforms, is located in the SW¼ Sec.30, T.25N., R.84W., Carbon County, Wyoming (Figs.1), 1,). The area is readily accessible via paved road by traveling north from the town of Sinclair, Wyoming, a distanceof 30 mi (48 km) on the Seminoe Road. This highway is the main access route to Seminoe State Park. The locale is on public land, administered by the Bureau of Land Management, but it borders on private ranch land to the north and state-owned land to the west.
The area is within the broad, windswept zone of central Wyoming (Fig. 1) known as the Wyoming Wind Corridor(Marrs and Kolm, Kolm 1982). The large active dunes at this site and older stabilized dunes in the area are part of the Seminoe Dune Field (Fig. 1) 2). Most dunes in the area are marginally stabilized parabolic dunes. The few active dunes are relatively large and slow moving with active fronts and partially stabilized tails.
The White River Badlands of South Dakota
Authors: Martin James E. 
Published: November 2007

Abstract
One of the most famous and spectacular Tertiary deposits in North America is the White River Badlands. The colorfully banded, fossiliferous, highly dissected landscapes are exposed across much of southwestern South Dakota; a specific landmark is difficult to designate. Most visitors to the Badlands traverse the area in the Badlands National Park between the towns of Interior and Wall in Pennington and Jackson Counties (Fig. 1). Most geological features may be viewed along South Dakota 240, the Badlands Loop; therefore this area has been designated a landmark. Geology is well-exposed along the route at such localities (Fig. 1) as the Pinnacles, Yellow Mounds, Rainbow Overlook, Banded Buttes Overlook, and Cedar Pass. Due to space limitations herein, frequent references are made to the road log, photographs, and bibliographic references of the area by Martin (1985).
Metamorphic, igneous, and sedimentary relationships on the Sioux Quartzite Ridge, South Dakota
Authors: Bretz Richard F. 
Published: November 2007

Abstract
The Sioux Quartzite Ridge geological site consists of three stops east and northeast of Sioux Falls, Minnehaha County, South Dakota, on the Sioux Falls 1° × 2° topographic map (Fig. 1). Sioux Falls is the starting point for a visit to these stops, which are east of the city on 1–90. All of the stops are on allweather roads, and can be reached by large groups traveling by bus. These stops are included in a longer field trip guide (Brenner and others, 1981), which contains more detail and further references.
Stop 1, the 1–90 section, is about 0.5 mi (0.8 km) east of the Corson-Brandon interchange, where the Interstate crosses Split Rock Creek (NE¼NE¼SW¼Sec.26, T.102N., R.48W.; Brandon 7½-minute Quadrangle). Since parking is not allowed on the interstate highway, park at the interchange and walk to the exposures, which occur both north and south of the highway. The outcrops are on private land owned by Howard R. Johnson, Corson, South Dakota 57019, telephone (605) 582–3898.
To reach the second stop, proceed 3.5 mi (5.7 km) to Exit 410 leave 1–90, turn left (north) onto the county road. Travel 5.8 mi (9.5 km) north and turn left (west) onto a gravel road. Proceed for 1 mi (1.6 km) and turn left (south), following signs to Palisades State Park. Drive 0.1 mi (0.2 km) farther and turn right (west) onto the road that leads into the state park.
Stop 2. Palisades State Park is publicly-owned land, so access is unlimited. A
The Book Cliffs Cretaceous section
Authors: Rigby J. Keith , Russon Michael P. , Carroll Richard E. 
Published: November 2007

Abstract
Location and Access. A classic cross section through Cretaceous and early Tertiary rocks is well exposed along U.S. 50-6 in Price Canyon, a gorge cut through the Book Cliffs of eastern Utah (Fig. 1). Price Canyon occurs, in part, on the Helper, Standardville, and Kyune 7½-minute Quadrangles, in northern Carbon County and southeastern Utah County.
Most significant outcrops are readily available along the highway on land controlled by the Utah State Highway Commission. Land beyond the right-of-way is privately owned in the lower part of the canyon, from Castlegate southward, but above Castlegate it is controlled by the Bureau of Land Management.
Significance. Roadside exposures up Price Canyon provide an almost totally exposed section from the middle of the Late Cretaceous Mancos Shale up to the Paleocene-Eocene Flagstaff and Colton Formations (Fig. 2). These outcrops show threedimensional relationships of open marine, deltaic and piedmont systems of the western margin of the Cretaceus Interior Seaway. The section provides excellent models for interpreting deposition in such environments and records a generally regressive elastic sequence. Relationships of major coal accumulation to these depositional environments are also clearly exposed in and near Price Canyon.
Previous Work. Geologic investigation in the area began more than 80 years ago. Numerous reports that concern the area are listed in Cross et al. (1975); Balsley ( 1982); Fouch and others(1983); and Russon (1986). Fouch and others (1983) summarized regional patterns of deposition of Late Cretaceusrocks of
Exceptionally fossiliferous Lower Ordovician strata in the Ibex area, western Millard County, Utah
Authors: Hintze Lehi F. 
Published: November 2007

Abstract
Exposures of the most richly fossiliferous Lower Ordovician strata in the United States occur about 50 mi (80 km) west of Delta, Utah, and extend over an area 6 by 8 mi(15 by 20 km). These rocks form low-lying hills in the southern part of the House and Confusion ranges (Fig. 1) and are reached by paved U.S. 6–50, which passes along the northern edge of the Ibex area, named for a small ranch abandoned in the 1930s. The area is neither populated nor fenced and isused primarily for winter sheep grazing under administration of the U.S. Bureau of Land zones useful to Ordovician students throughout the world. Management, which maintains graded dirt roads that lead to within easy walking distance of most outcrops. There is no water.
The geology of Salina Canyon, Utah
Authors: Lawton Timothy F. , Willis Grant C. 
Published: November 2007

Abstract
The spectacular exposures in the lower part of Salina Canyon(Figs. 1, 2) lie in the Basin and Range to Colorado Plateau transition zone to the east of thrust-faulted Paleozoic rocks in the Pavant and Canyon ranges. The stratigraphic and structural relations exposed along a 4-mi (6.5-km) east-west corridor here provide unsurpassed insight into the late Mesozoic to middle Tertiary geologic history of central Utah. A well-exposed Middle Jurassic to Upper Cretaceus sedimentary section is unconformably overlain by one of the most complete lower Tertiary sequences found in this part of the state.
The site can be reached by following old U.S. 50 (called the “frontage road” in this text) from Salina or from the Gooseberry Valley exit off 1–70 east of the site (Fig. 1, inset). Examination of the area requires two short hikes, one of about 1 mi (1.6 km) round trip (depending upon your vehicle) and one of 2.5 mi(4.0 km).
Late Paleozoic-Mesozoic stratigraphy, Hite region, Utah
Authors: Baars D. L. 
Published: November 2007

Abstract
Present-day Hite, Utah, is on the east bank of Lake Powel in the Glen Canyon National Recreation Area of southeastern Utah (Fig. 1F). It is in T.33 S., R. 14 E., on the Browns Rim 15-minute Quadrangle, San Juan County, Utah. Hite Crossing bridge over the Colorado River extension of Lake Powell ( Fig. 2)is about 75 mi (120 km) west of Blanding, Utah, and 48 mi (77km) southeast of Hanksville, Utah, along Utah 95. The present site of Hite, relocated when Lake Powell flooded the Colorado River canyons, is at about 3,960 ft (1,200 m) near the mouths of White Canyon, entering the Colorado River from the southeast, and the Dirty Devil River and North Wash, entering from the northwest. Access is best shown on the Hite Crossing 1:100,000 map. The area is readily accessible via Utah 95 and is entirely on public lands, either Glen Canyon National Recreation Area or Bureau of Land Management administered lands.
The Milk River Canyon, Alberta
Authors: Beaty C. B. , Barendregt R. W. 
Published: November 2007

Abstract
The Milk River Canyon is located in southeastern Alberta some 62 mi (100 km) east of the town of Coutts (Fig. 1). Access to a valley overlook by passenger caron paved and unpaved county roads is relatively easy and requires no permissions to cross private land, but the easternmost unpaved section of road (beyond Black Butte, Fig. 2 is to be avoided if wet. The canyon itself is not visible until the overlook on its rim is reached. The map (Fig. 2 shows readily recognizable points on the route from Coutts and indicates distances between conspicuous landmarks. As is customary, barbed wire gates, if encountered, should be left as found: open if open, closed if closed. There are no services available east of Coutts, so gas tanks should be comfortably filled.
Tertiary mineralization—Idaho Springs, Colorado
Authors: Budge S. , LeAnderson P. J. , Holden G. S. 
Published: November 2007

Abstract
As 1–70 climbs westward from Denver to the Continental Divide, it traverses the Idaho Springs, Central City, Empire, Georgetown, and Silver Plume mining districts, which lie near the northeast end of the Colorado Mineral Belt. Together these districts comprise a zone of nearly continuous mineralization extending about 16 mi (27 km) east-northeast from Silver Plume to Central City. Originally gold, then later Ag, Cu, Pb, Zn, and U were produced from the area, beginning in 1859. Most mines at present are inactive. Primary precious-metal production was dominated by gold, with some silver, from the Idaho Springs and Central City districts to the northeast and mainly by silver from the Silver Plume and Georgetown Districts to the southwest.Mineralization was associated with shallow Tertiary igneous activity in country rockcomposed of Precambrian (middle Proterozoic) granite and gneiss.
The Idaho Springs site is one of the few easily accessible locations where the Tertiary intrusive suite and mineralization are well exposed on the surface. The site is a road cut along the north side of 1–70, just west of Idaho Springs (Fig. 1). A sketch, drawn to scale, is provided to show the features that may be observed (Fig. 2) 2). Access to the outcrop is along a 20-ft (6-m) wide service road protected from 1–70 by a guardrail.
The Black Canyon of the Gunnison, Colorado
Authors: Hansen Wallace R. 
Published: November 2007

Abstract
The Black Canyon in southwestern Colorado is easily reached by passenger car from U.S. 50 (Fig. 1). Turn north 8 mi (13 km) east of Montrose, Colorado, to reach Black Canyon of the Gunnison National Monument in the most impressive part of the canyon. The National Monument boundary is 5 mi (8 km)from the turnoff, and the approach is very scenic. A key visitation point in the monument is Chasm View overlook. Most visitors will want to see several other points also. Some parts of thecanyon are accessible only by 4-wheel-drive trails or footpaths.
The carbonatite complex at Iron Hill, Powderhorn district, Gunnison County, Colorado
Authors: Armbrustmacher Theodore J. , Shannon Spencer S. 
Published: November 2007

Abstract
The carbonatite complex at Iron Hill is located southeast of the town of Powderhorn along Cebolla Creek, Deldorado Creek, and Beaver Creek in Gunnison County, Colorado. To reach the complex, travel 9 mi (14.5 km)west of Gunnison on U.S. 50 to the intersection with Colorado 149, turn south on Colorado 149 and travel 15 mi (24 km) to the intersection with Cebolla Creekroad; turn southeast on Cebolla Creek road; after about 2.5 mi (4km), the outcrops on the left are in the carbonatite stock of the Present address: Department of Geology, Adams State College, Alamosa, Colorado 81102 complex. Roads to the east off Cebolla Creek road along Deldorado Creek and Beaver Creek connect with a variety of dirt ranch roads that provide excellent access to the rocks of the complex.These roads are periodically maintained by Humphreys Mineral Industries, Inc., of Denver, Colorado, the property managers.Therefore, most of the complex is easily accessible by short hikes from roads navigable by most vehicles. A number of patented mining claims exist in the area, but permission to access the property has never been denied. The geologic map of the complex(Fig. 1) is located within the Rudolph Hill Quadrangle(Olson, 1974) and within the Powderhorn Quadrangle (Hedlund and Olson, 1975).Access roads are also shown on the Rudolph 325 Hill and Powderhorn 7.5-minute quadrangles (1:24,000). Some of the better localities at which to see specific rock exposures are shown on Figure 1.
Multiple catastrophic drainage of Glacial Lake Missoula, Montana
Authors: Alt David D. 
Published: November 2007

Abstract
The lake-drainage site is in Sanders County, Montana, approximately 65 mi (105 km) northwest of Missoula, and about the same distance southwest of Kalispell (Fig. 1).
Paved, two-lane highways and easily passable side roads provide interconnecting access to most parts of the area at all seasons. Montana 382 between Perma and its junction with Montana 28 passes through Markle Pass and across the giant ripples of Camas Prairie. An unpaved track leads from that road to Wills Creek Pass and the Schmitz Lakes. Montana 28 between Plains and Hot Springs crosses the debris fill in the valley of Boyer Creek, and passes Rainbow Lake and through Duck Pond Pass above its head. An unpaved county road connects Rainbow Lake and Camas Prairie.
Ownership is a mixture of private ranch land, public and private forest land, and Flathead-Salish tribal lands, none of which are posted. Access is generally open to all parts of the area except that people planning to spend significant amounts of time on the tribal lands around Rainbow Lake should buy a recreation permit.
The varve site comprises large roadcuts through stream and glacial lake deposits on and near 1-90 in the vicinity of the Nine-mile Exit, about 19 mi (31 km) west of Missoula, in Missoula County (Fig. 1).