bluuebunny/crossref_metadata_2025_split huggingface dataset:
Copperas Mountain
Authors: Carlson Ernest H. 
Published: November 2007

Abstract
Copperas Mountain is located on the south side of Paint Creek Valley in southwestern Ross County, south-central Ohio (Fig. 1). Erosion by Paint Creek has produced a steep face along the northwestern side of this northerly trending ridge that forms one of the most remarkable exposures in the state (Fig. 2). The site is reached by traveling southwest on U.S. 50 from Bourneville for 1.0 mi (1.6 km), turning south on Jones Levee Road for 0.9 mi ( 1.5 km), continuing west on Spargursville Road for 1.5 mi (2.2 km), turning west and following Orms Road and then Storm Station Road for 0.7 mi (1.2 km), and finally bearing sharply west onto a narrow township road for 0.7 mi (1.2 km) (Figs.1, 2). Vehicles should be parked at the side of the road just north of the cliff, as the road at the foot of the cliff is narrowand treacherous. The cliff area is particularly hazardous in the spring and after periods of rain, due to slick rock and rock falls. The road provides access to the lower portions of the section, while trails lead to the upper parts of the face.
Glacial and interglacial stratigraphy, Hudson Bay Lowlands, Manitoba
Authors: Dredge L. A. , Nielsen E. 
Published: November 2007

Abstract
Extensive sections along the Nelson River in northern Manitoba lie within NTS sheet 54 D (1:250,000). The nearest town, Gillam, can be reached by air or road from Winnipeg, Manitoba.From Gillam, follow the road eastward across Long Spruce Dam and proceed toward Sundance. Access to each site (Fig. 1) is obtained by parking the vehicle along the roadside and walking a very short distance to the bluff.
The Serpent Mound disturbance, south-central Ohio
Authors: Koucky Frank L. , Reidel Stephen P. 
Published: November 2007

Abstract
The Serpent Mound disturbance is located at the common boundaries of Adams, Pike, and Highland countiesin southcentral Ohio (Fig. 1). The locality lies on the eastern edge of the Interior Low Plateau province and just west of the Appalachian Plateau. Serpent Mound State Memorial, a prehistoric Indian site of the Adena culture, is situated on the west side of the disturbance above Ohio Brush Creek. Two paved highways serve the area; all other roads within the disturbance are gravel. Ohio 73 crosses the southwest part of the disturbance, providing access to the Serpent Mound State Memorial, and Ohio 41 passes through the east side of the disturbance (Fig. 2). Pertinent 7½-minute Quadrangles are the Byington and Sinking Spring sheets.Access to most geologic sites within the area is by foot. All land within the disturbance is privately owned, and permission must be gained to visit it. Landowners, however, understand the scientific significance of the area and have granted access graciously.
Seagull Lake-Gunflint Lake area
Authors: Miller J. D. , Morey G. B. , Weiblen P. W. 
Published: November 2007

Abstract
The Seagull Lake-Gunflint Lake area along the Gunflint Trail (Cook County Highway 1) in T. 65N., R. 3 and R. 4W. in the northwestern part of Cook County, Minnesota (Fig. 1) is north of Grand Marais, the county seat and starting point for the Gunflint Trail. Although accessible by automobile or bus, much of the site is rugged and heavily wooded and requires considerable off-road travel. Except for obvious resorts and summer homes, the site is on public lands managed by the U.S. Forest Service.
There is no single place where the entire geologic succession is laid out for easy study, so one must visit several localities to appreciate the significance of the area. This guide suggests 12 stops (Figure 2) that can be easily visited in one day and that collectively illustrate the major rock types and their stratigraphic and structural attributes. However, exposureis of such quantity and quality that independent exploration is heartily encouraged.
Late Cretaceus strata exposed at Ponca State Park, Dixon County, Nebraska
Authors: Pabian Roger K. , Lawton Dennis R. 
Published: November 2007

Abstract
The outcrops of the Dakota Group and the Graneros Shalenental sandstones. As the viewer examines younger rocks toward Greenhorn Limestone interval of LateCretaceus age at Ponca the northwest, the original environments of deposition change, State Park provide an excellent sedimentary record of the last and these deposits give way to lagoonal, estuarine, or tidal and great marine invasion of the North American midcontinent. The mudflat deposits, which are finally overwhelmed by marine southeastern end of the outcrop area consists of the older continental sandstones. As the viewer examines younger rocks toward. the northwest, the original environments of deposition change, and these deposits give way to lagoonal, estuarine, or tidal and mudflat deposits, which are finally overwhelmed by marine shales and limestones.
The Ordovician Sequence in the Gutenberg Area, northeast Iowa
Authors: Witzke Brian J. , Glenister Brian F. 
Published: November 2007

Abstract
Gutenberg is a picturesque community nestled in the Mississippi River Valley, where local relief approaches 400 ft (120 m). Lock and Dam No. 10 at Gutenbergis a major conduit for upper Mississippi barge traffic. Visitors can view the lock in operation at close range from an observation platform.
Excellent roadcuts and many additional exposures of Middle Ordovician strata are easily accessible in the Gutenberg area, where virtually every bed is available in continuous fresh exposures over a stratigraphic interval of more than 250 ft (75 m).Three reference sections (Fig. 1B) enable the sequence of Ordovician formations (St. Peter, Glenwood, Platteville, Decorah, Dunleith, Wise Lake) to be composite for general discussion (Fig. 2) :1) Gutenberg South Roadcut, US. 52 (SW¼Sec.29, T.92N., R.2W.), a superb continuous section that offers a spectacular view of the Mississippi River (Delgado, 1983); 2) Gutenberg North Roadcut, U.S. 52 (SW¼SW¼Sec.5 and NW¼Sec.8, T.92N., R.2W.), a well-studied but now partly overgrown sequence (Templeton and Willman, 1963; Bakush, 1985); and 3) X56 Roadcut, Great River Road (NW¼NW¼Sec.32 and SW¼SW¼Sec.29, T.93N., R2W.), a similar sequence to Gutenberg North, but better exposed by recent road construction. Excellent exposures of Lower and Middle Ordovician rocks are also accessible at Clayton (especially private barge terminal road) and the Pikes Peak State Park area (Fig. 1A). Good exposures of Jordan Sandstone (Cambrian) can be seen along the river from McGregor north to Effigy Mounds (Fig. 1A).
Ordovician stratigraphic terminology in
Pennsylvanian deformation and Cambro-Ordovician sedimentation in the Blue Creek Canyon, Slick Hills, southwestern Oklahoma
Authors: Donovan R.N. , Ragland D. , Rafalowski M. , McConnell D. , Beauchamp W. , Martini W. R. , Sanderson D. J. 
Published: November 2007

Abstract
Blue Creek Canyon is located approximately 15 mi (24 km) north-northwest of Lawton in southwestern Oklahoma (T.4N., R.13W.). Oklahoma 58 (Fig. 1) runs through the canyon. The area can be most easily reached from Lawton by taking the Medicine Park exit from the H. E. Bailey Turnpike a few miles north of Lawton.
The entire area described here is part of the Kimbell Ranch, owned by Mr. and Mrs. David Kimbell of Wichita Falls. The ranch house is situated at the south end of the canyon (Fig. 2) and is managed by Charlie Bob and Dixie Oliver. Both the Olivers and the Kimbells have greatly encouraged the visits of geologists, and several local universities use the area as a student training ground. Permission to visit should be sought from Mr. Oliver, and the usual common sense and courtesy extended. The ranch address is Star Route A, Box 124, Lawton, OK 73501. The Olivers carry their interest in geology to a remarkable level; during monitoring of the recently active Meers Fault, they had a seismograph installed in their bedroom as part of a regional network.
The descriptions in this field guide are for a series of walks that start approximately 0.5 mi (0.8 km) north of the ranch house at Red Hill (a small hill of Carlton Rhyolite capped by Post Oak Conglomerate which is immediately west of the road) (Fig. 2). The walks are all rough and fairly hilly; exposure is more or less continuous. The area is well drained
Beaver Dam, northwestern Arkansas
Authors: Manger Walter L. 
Published: November 2007

Abstract
The Beaver Dam exposure is reached by taking Arkansas 187 south from its junction with U.S. 62 immediately south of Busch, Arkansas (Fig. 1). Arkansas 187 crosses Beaver Dam and a turnoff to the dam site overlook is located approximately 0.25 mi (0.4 km) south of the dam. Parking maybe found at the overlook. This exposure occupies NW¼Sec.10, T.20N., R.27W., Carroll County, Arkansas.
Peyton Creek Road Cut, northern Arkansas
Authors: Manger Walter L. 
Published: November 2007

Abstract
Road cut on east side of U.S. 65 beginning directly south of the Peyton Creek Bridge, 0.2 mi (0.3 km) south of the Searcy- Van Buren county line and 3.4 mi (5.5 km) south of Leslie. NE¼, Sec.11 and NW¼, Sec.12, T.13N., R.15W., Van Buren County, Arkansas (Fig. 1).
Blue Mountain Dam and Magazine Mountain, Arkansas
Authors: Cohoon Richard R. , Vere Victor K. 
Published: November 2007

Abstract
Blue Mountain Dam can be reached by driving east 17 mi (27 km) from Bonneville, Arkansas, on Arkansas 10 to Waveland, and then turning south on Arkansas 309 for 0.8 mi (1.3 km) to the entrance to the Waveland Recreation Area. Turn west on the entrance road and follow the road over the spillway bridge and dam to the outcrops at the south abutment of the dam (Fig. 1).
Magazine Mountain can be reached by continuing east 6.4 mi (10 km) from Waveland on Arkansas 10 to Havana. At Havana, take Arkansas 309 north 4.9 mi (8 km) to Stop 2 on the flanks of Magazine Mountain (Fig. 2). To reach Stop 3, continue along Arkansas 309 for 3.6 mi (5.8 km). Stop 4 is 0.5 mi (0.9 km) farther along the road, at the top of the mountain.
Late Paleozoic rocks, eastern Arkoma basin, central Arkansas Valley Province
Authors: Kehler P. L. 
Published: November 2007

Abstract
A late Paleozoic section, as well as structures and geomorphology typical of the Arkansas Valley Province and the Frontal Ouachita Mountain Province are demonstrated by a transect extending from near Morrilton, Conway County, Arkansas to near Perryville, Perry County, Arkansas (Fig. 1).
Geological features at Hot Springs, Arkansas
Authors: McFarland J. D. 
Published: November 2007

Abstract
The area in and around Hot Springs National Park offers many tine exposures of Ordovician through Mississippian reeks along with some recent formations particular to the thermal springs (Stone and Bush, 1982). These strata are often steeply inclined to overturned, with many tight folds and numerous thrust faults formed by the late Paleozoic orogeny that uplifted the Ouachita Mountains. These rocks often contain quartz veins, small Cretaceous-age igneous dikes, and both hot and cold springs. The units to be examined in this area include the Middle Ordovician age Bigfork Chert, the Upper Ordovician age Polk Creek Shale, the Silurian-age Missouri Mountain Shale, the Devonian-Mississippian Arkansas Novaculite, and the Missis-sippian-age Stanley Shale (including the Hot Springs Sandstone Member). Roads that lead up to the crest of Hot Springs Moun-tain and West Mountain have several lookouts that provide viewsof the surrounding countryside. A high tower on Hot Springs Mountain is an excellent place to view the wide Mazarn Basin (a synclinorium underlain by Mississippian age Stanley Shale), the distant Trap Mountains (formed mostly by the Devonian-Mississippian Arkansas Novaculite), the Zigzag Mountains (Ar-kansas Novaculite and other formations), and the “core’ area of the Ouachita Mountains (an anticlinorium with extensive expo-sures of Ordovician sediments).
The Eocene Jackson Group at White Bluff, Arkansas
Authors: Colton George W. , Bush William V. 
Published: November 2007

Abstract
White Bluff is immediately north of Lock and Dam No. 5, about 15 mi (24 km) upriver from the city of Pine Bluff, Jefferson County, Arkansas. The best method to reach the bluff is by boat along the Arkansas River. Launching ramps are available at the Tar Camp Public Use Area, approximately 1.5 mi (2.4 km) upriver from White Bluff. Tar Camp Public Use Area is accessible via Redfield River Road from Redfield, which is on Arkansas 365. U.S. 65 parallels Arkansas 365 and the two are connected by Arkansas 46 (Fig. 1). Access to the top of the cliffs from the west is not recommended because of their steepness and the uncertain footing on the poorly consolidated materials. Other excellent exposures of the Jackson are present in less-steep cliffs on the west bank of the river at Red Bluff and South Red Bluff, approximately 2 mi (3.2 km) to the north (Fig. 1).
The Lingos formation, western Rolling Plains of Texas
Authors: Caran S. Christopher , Baumgardner Robert W. 
Published: November 2007

Abstract
Lingos strata (Figs. 1, 2) are well exposed at localities in Hall, Briscoe, and Floyd counties, Texas. Except where the formation is dissected or where remnants of bedrock project through it, the Lingos terrane is a smooth continuous geomorphic surface sloping southeastward approximately 80 ft/mi (15 m/km) near the escarpment and 40 ft/mi (7.5 m/km) farther east. The route between the Field Guide localities described here crosses this geomorphic surface, within the area covered by the Plainview sheet of the Geologic Atlas of Texas (Barnes, 1968). However, none of the deposits now recognized as the Lingos formation are shown on the atlas or other maps published before 1984. Topographic maps (7½-minute) covering the localities in this Field Guide are: Turkey, Folley, Quitaque and Lake Theo.
Late Pleistocene and Holocene stratigraphy, Southern High Plains of Texas
Authors: Holliday Vance T. 
Published: November 2007

Abstract
Begin in Crosbyton, Texas (Fig. 1). Take U.S. 82 west 35 mi (56 km) to Lubbock. On the northeast side of Lubbock at the intersection of U.S. 82 (which is also U.S. 62 along this stretch of the road) and Loop 289, turn right (north) off of U.S. 82 and follow Loop 289 to the north and west. Cross over I-27/U.S. 84, and take the University Avenue exit. Stay on the frontage road and continue west, parallel to the loop. Cross University Avenue and continue west with the large Texas Instruments (TI) plant to the north (right). Just past the TI plant the road drops into Yellowhouse Draw. The Lubbock Lake site, is in the trees to the northwest, about 300 ft (100 m) away. On the floor of the draw, take the only paved road north (right). Follow it for 0.3 mi (500 m) as it curves to the left along the edge of the draw. A chain-link fence enclosing most of the trees becomes visible. This is Lubbock Lake.
The Triassic section of the West Texas High Plains
Authors: Gawloski Ted 
Published: November 2007

Abstract
The Triassic section of the West Texas High Plains is represented by the rocks of the Dockum Group. This section consists of up to 2,000 ft (61 O m) of complex elastic sequence composed of conglomerates, sandstones, and shales. These sediments were deposited by a variety of terrigenous depositional systems into a broad, shallow, fluvial-lacustrine basin stretching across what is now the Panhandle region of Texas. The location and geometry of the Dockum Basin probably reflect Paleozoic structural elements lying in an area roughly defined by the Midland Basin. It is bounded to the north by the Sierra Grande Arch and Amarillo Uplift and to the south by the Llano and Marathon Uplifts (Fig. 1). Most of the Triassic deposits of West Texas occur beneath younger deposits of the Llano Estacado. These rocks crop out along the Caprock Escarpment from Oldham County southward to Sterling County (Fig. 1). Terminology applied to the Dockum Group of West Texas has undergone considerable evolution. Presently, the Dockum Group of the West Texas High Plains is divided into two formations. These are, from oldest to youngest, the Tecovas and Trujillo formations (Fig. 2). In the southern outcrop areas, however, the formational divisions are difficult to identify.
Middle and late Pennsylvanian rocks, North-Central Texas
Authors: Trite E. L. “Jack” , Grayson Robert C. 
Published: November 2007

Abstract
The middle and late Pennsylvanian (Desmoinesian-Missourian) section of north-central Texas is illustrated by a transect extending from eastern Parker County northwestward to northeastern Palo Pinto County (Fig. 1).
The transect begins in the Dobbs Valley Member of the Mingus Formation (middle Strawn Group, Desmoinesian; Localities 1 and 2) and crosses through the Brazes River Formation and Mineral Wells Formation (upper Strawn Group, Desmoinesian- Missourian; Localities 3 and 4), Palo Pinto Formation, Wolf Mountain Shale, and into the Winchell Limestone (Canyon Group, Missourian; Localities 5 and 6; Figs. 1, 2).
Strawn and Canyon reeks generally reflect the cyclic depositional nature of the Pennsylvanian. The vertical succession of these rocks illustrates the final filling of the Fort Worth Basin and cyclic fluvial/deltaic progradation and marine transgression of the epeiric sea over the Eastern Shelf (Fig. 3). A shelf edge into the Midland Basin developed in Missourian time. Slope and basin depositional systems are recognized in the subsurface in Missourian and Virgilian time. Sources for the clastics were the Quachita Mountains and Southern Oklahoma Mountains. This transect illustrates some of the major elastic and carbonate depositional systems in the Strawn and Canyon Groups.
The Comanchean Section of the Trinity shelf, central Texas
Authors: Hayward O. T. 
Published: November 2007

Abstract
This traverse is a composite of six localities (Fig. 1)—four in the Trinity Group and one each in the Fredericksburg and Washita Groups (Fig. 2)—exposed along a route extending from near Eastland (Eastland County) on the west to a point near Blum (northwestern Hill County) on the east, a straight-line distance of about 75 mi (120 km). The section transects the eastern margin of the Trinity Shelf and ends near the western margin of the East Texas Basin (Fig. 3). The section extends from the Western Cross Timbers across the Glen Rose Prairie, the Lampasas Cut Plain, and the Washita Prairies, which together make up the Grand Prairies of Texas (Hill, 1900) (Fig. 4).
Gulfian rocks, western margin of the East Texas Basin
Authors: Hayward O. T. 
Published: November 2007

Abstract
The Gulfian section of Central Texas is illustrated by a transect extending from northwestern Hill County southeastward to northeastern Limestone County (Figs. 1 to 6). This transect begins in latest Washita rocks of Comanchean age (locality 1; Figs. 1, 3), and crosses in succession the outcrop belts of Woodbine Sand (localities 1 and 2; Fig. 3); Eagle Ford Group (locality 3; Fig. 4); Austin Chalk (locality 4; Fig. 4); Taylor Group (locality 5; Fig. 5); and Navarro Group, all of Gulfian age, to end at the Midway Group (locality 6; Fig. 6) of Paleocene Age (Hill, 1901; Adkins, 1933; Bureau of Economic Geology, 1970, 1972). Structurally, it originates near the eastern margin of the Central Texas Platform (Fig. 3), and trends downdip across the northern end of the Balcones Fault Zone (Fig. 4) into the East Texas Basin (Fig. 3), to terminate in the Mexia Fault Zone (Fig. 6; Oliver, 1971). Geomorphically it begins at the eastern margin of the Grand Prairies (Fig. 3), and crosses the Eastern Cross Timbers and the Black Prairies (Figs. 4,5, 6) to end at the western margin of the East Texas Timber Belt (Fig. 6; Hill, 1901 ). Throughout this route, the geology, landscape, history, and land use are clearly related.
Paleozoic strata of the Llano region, Central Texas
Authors: Kier Robert S. 
Published: November 2007

Abstract
The Paleozoic rocks of central Texas occur in the numerous fault blocks that compose the Llano uplift, also known as the Central Mineral Region, a structural high in the Precambrian basement centered in Llano County, northwest of Austin (Fig. 1). The predominant trend of the fault blocks is southwest to northeast. For the most part, the Paleozoic rocks are preserved in grabens. Few fault blocks are large enough, however, to display the entire Paleozoic section; thus, no single transect can be made that will allow a view of the entire section. Rather, the Paleozoic section must be examined at a number of isolated localities from which a regional picture can then be formulated. Rapid facies changes in some of the formations compound the difficulty of piecing together a representative section. The Brownwood and Llano sheets of the Geologic Atlas of Texas (Barnes and others, 1976, 1981) cover the entire area of interest.
Most of the localities are along roadcuts where access presents no problem; possible restrictions on public access to locality 7 are noted. Because of access problems, no localities are presented for the thin, patchy Upper Ordovician, Silurian, and Devonian formations, few of which are in normal stratigraphic position. Most of these are preserved in collapse structures, sinks, and crack fillings.
Enchanted Rock dome, Llano and Gillespie counties, Texas
Authors: Hutchinson Robert M. 
Published: November 2007

Abstract
Enchanted Rock dome is centrally situated in Texas (Fig. 1) and is easily accessible via state asphalt roads. The site is maintained year long, and for a small fee the visitor can climb to the top of the dome. The site can be reached by driving 17 mi (27.4 km) north from Fredericksburg on Texas 965 or south from Llano 15 mi (24.1 km) to the intersection of Texas 965. From there it is 8 mi (12.9 km) to the site. The exfoliation dome is the largest of five domes extending in a line for 1.75 mi (2.82 km) along the west side of Sandy Creek. The dome covers an area 0.4 x 0.6 mi (0.64 x 0.96 km) and is 425 ft ( 129.5 m) high. Granitetectonic features of the dome can easily be seen in half a day (Fig. 2).
Basal Gulfian and Comanchean Section, Anguila Fault Zone and Santa Elena Canyon, Big Bend National Park, Trans-Pecos Texas, and Chihuahua, Mexico
Authors: Stevens J. B. 
Published: November 2007

Abstract
Santa Elena Canyon and the Anguila Fault Zone northwest of the canyon are occupied by the Rio Grande. These features separate Mesa de Anguila, the westernmost part of Big Bend National Park, Brewster County, Texas, from northeastern Chihuahua, Mexico (Fig. 1). The traverse begins on the river at Lajitas (reached by FM 170), southwestern Brewster County, about 2 mi (3.2 km) above the entry to an upper canyon, and ends at the lower end of Santa Elena Canyon, where Terlingua Creek joins the Rio Grande from the northwest. This location is accessible by a paved park road. The canyons are accessible only by river, a trip best made in a sturdy rubber raft. Travel through the canyons is strictly regulated by the Big Bend National Park administration, particularly with respect to safety equipment and camping. Permits may be obtained at a ranger station at Lajitas, or at park headquarters at Panther Junction. The simplest procedure is to arrange a guided tour through businesses in Lajitas, Terlingua Ghost Town 12.5 mi (20.1 km) east of Lajitas on FM 170, or Study Butte (junction of Texas 118 and FM 170) 16.9 mi (27.2 km) east. A permit is necessary to collect rock samples in any national park; even if the intent is to restrict sampling to the Mexican side of the river, it would be best to obtain such a permit. Santa Elena Canyon and the lesser (but still impressive) canyon immediately upstream provide access at and near river level to virtually