bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Claiborne Group in southwest Arkansas
Authors: Prior William Lee , Baber Quin 
Published: November 2007

Abstract
Although the middle Eocene age Claiborne Group of southwest Arkansas covers a large area, outcrops are sparse. The easily erodable Claiborne is composed of unconsolidated sand, silt, clay, and lignite. It has a maximum thickness of 1,500 ft (457 m) in Arkansas, generally strikes to the northeast, and dips an average 60 ft to the mi (11 m to the km) to the southeast. The exposures at Camden and Red River in southwestern Arkansas (Fig. 1) display features of a deltaic plain environment. The two exposures are 75 mi ( 120 km) apart and are probably of different parts of the Claiborne section. Currently, the Claiborne Group is interpreted as having accumulated in fluvial-deltaic system. Studies by Bernard and others (1970) have established a classification scheme of sedimentary environments within deltas. Texture, fabric, sedimentary features, geometry, and trends of sediments associated with deltas are controlled by geologic processes and the availability and influx of different sediment types. Based on these criteria, delta depositional environments have been divided into (1) delta plain with natural levees, distributary channels, interdistributary marshs, and flood basins; (2) inner fringe with rivermouth bars; (3) outer fringe; (4) prodelta; and (5) open marine (Figs. 2 and 3). These environments are discussed within the context of high sediment influx, low energy type of coastal delta (birdfoot, lobate) interpretation of the Claiborne Depositional system, as opposed to low sediment, high coastal energy deltas (arcuate, estuarine).
Permian strata of North-Central Texas
Authors: Jones James O. , Hentz Tucker F. 
Published: November 2007

Abstract
Permian sedimentary rocks of North-Central Texas are exposed in a northeast-striking outcrop belt that extends from overlying Cretaceus strata composing the Edwards Plateau in the south to the Red River and Panhandle region in the north. The gently inclined (0.50), west-dipping Permian strata, over 5,500 ft (1,680 m) of section, are represented in this chapter as a transect of about 180 mi (290 km) in the northern part of the outcrop area (Fig. 1).
The Claiborne Group of East Texas
Authors: Sharp Patricia S. , Sartin Austin A. 
Published: November 2007

Abstract
An ancestral coastal plain was the principal setting for the deposition of the Claiborne Group. Units within the Claiborne dip to the southeast at one to two degrees. Generally the Claiborne formations crop out in an arcuate pattern across the east Texas area, with the older formations cropping out farther to the north and west while the younger formations crop out nearer to the present coast.
The ancestral coastal plains area of Texas consists of several major structural features: Sabine Uplift in extreme East Texas, Tyler Basin in east Texas, San Marcos Arch in central Texas, and Rio Grande Embayment in southern Texas (Fig. 1). Formation of these structural features influenced the deposition of the Claiborne units. High areas, such as the Sabine Uplift and the San Marcos Arch, caused rivers to reroute and diverge their courses. This resulted in minimal amounts of material being deposited in those areas of uplift. Subsidence created the basinal features such as the Tyler Basin and Rio Grande Embayment, and great thicknesses of material were deposited in these susiding lows. Normal faulting has vertically displaced the Claiborne units throughout the area.
Claiborne exposures discussed here are located within approximately 6 mi (10 km) of Jacksonville, Texas, in Cherokee County (Fig. 2). Outcrops that primarily expose the Queen City and Weches formations are easily accessible along U.S. 69 north and south of Jacksonville and along U.S. 79 west of Jacksonville. In several localities, upper and lower contacts of the Queen City and Weches formations are visible. The formations are
Cambrian algal reefs of the upper Wilberns Formation, central Texas, The Camp San Saba locality
Authors: Ahr Wayne M. 
Published: November 2007

Abstract
The famous algal reefs of the upper Wilberns Formation in central Texas are well illustrated by the section at the Camp San Saba crossing on the San Saba River, McCulloch County, Texas (Figs. 1, 2). These reefs are entirely within the San Saba Member of the Upper Cambrian Wilberns Formation (Barnes and Bell, 1977).
The Precambrian of Central Texas
Authors: Barnes Virgil E. 
Published: November 2007

Abstract
“Precambrian rocks reach the surface in the Llano region of Central Texas in the highest part of a broad domal arch, the Llano uplift, which appears on a regional geologic map as an island of igneous and metamorphic rocks surrounded by Paleozoic and Cretaceus sedimentary rocks. The widest expanse of Precambrian rocks is about 65 mi ( 105 km), extending westward from the valley of the Colorado River through a subdued topographic basin drained by the Llano River. The broad, gentle basin carved into the Precambrian rocks is bordered by a discontinuous rim of flat-topped limestone hills which are the dissected edge of the Edwards Plateau. Within the basin and at its margins are erosional remnants and down-faulted blocks of Paleozoic rocks which form prominent hills, locally referred to as mountains.” Clabaugh and McGehee (1972, p. 9).
The main Precambrian units present in the Llano region are listed in Table 1, and the distribution of some of these units is shown in Figure 1. This figure is derived from the Llano Sheet of the Geologic Atlas of Texas, scale 1:250,000 (Barnes, 1981). On that map (as well as Fig. 1), the Oatman Creek and Sixmile Granites (Table 1) are lumped as younger granitic intrusive rocky locally, in the southeast part of the Llano Sheet, the Packsaddle Schist is subdivided into four formations (McGehee, 1979). Detailed 7½-minute quadrangle maps include most of the area in which the Packsaddle Schist has been subdivided (Barnes and McGehee, 1976; 1977a, b, c).
The Catahoula Formation; A volcaniclastic unit in east Texas
Authors: Ledger Ernest B. 
Published: November 2007

Abstract
The Oligocene/Miocene Catahoula Formation of the upper Texas coastal plain is a fluvial and lacustrine volcaniclastic unit composed of “normal” quartz-rich fluvial material mixed with distal rhyolitic air-fall ash from coeval volcanic source areas in Trans-Pecos Texas and northern Mexico. It consists of poorly sorted siltstones, sandstones, and mudstones. The silt-size fraction includes abundant, slightly altered, volcanic glass shards. Sandsize grains are mostly quartz, some of which are very coarse—the “rice sands”. The clay-size fraction is montmorillonite, an alteration product of the glass.
The narrow outcrop belt of the Catahoula Formation, which is somewhat less than 300 ft (100 m) thick in Jasper County, extends from central Mississippi, through Louisiana and Texas parallel to the present coastline, and into eastern Mexico where it is not well studied.
Catahoula deposition is characterized by sporadic influxes of air-fall ash into low-gradient fluvial and coastal lake environments. Stratigraphic studies of the Catahoula Formation began as early as 1857, and the formation has since been studied by numerous stratigraphers and sedimentologists, including Hilgard, Penrose, Dumble, Veatch, and Deussen. Dumble (1918) gives a summary of this earlywork. Bailey (1926) named the lateral equivalent in the lower Texas coastal plain of south Texas theGueydan, and along with Renick (1936) established the Catahoula as a mid-Tertiary fluvial unit with abundant volcaniclastic material. A more recent summary of stratigraphic nomenclature is given in Sheldt (1976). Other recent studies of the Catahoula are concerned with petrology, geochemistry, and uranium ore genesis.
Geology of the Marathon Uplift, west Texas
Authors: McBride Earle F. 
Published: November 2007

Abstract
Roadcuts provide the only exposures of public access in the Marathon Uplift. However, roadcuts on U.S. 385 south of the town of Marathon and on U.S. 90 east of Marathon display spectacular features. Mileages to the first five stops in this guide are given from the junction of U.S. 385 south and U.S. 90 at the west edge of Marathon; mileages to the six remaining stops are from the junction of U.S. 385 north and U.S. 90 (Fig. 1).
Persimmon Gap in Big Bend National Park, Texas; Ouachita facies and Cretaceus cover deformed in a Laramide overthrust
Authors: Tauvers Peter R. , Muehlberger William R. 
Published: November 2007

Abstract
Persimmon Gap is unique in that the effects of three major Persimmon Gap. A wind gap that was part of the historic orogenies are exposed. A Paleozoic inlier features the southern- Comanche Trail crosses the southern Santiago Mountains at the most exposed thrust faults (Upper Ordovician over Lower Pennnorthern entrance to Big Bend National Park. The Persimmon sylvanian) of the Ouachita system in Texas. These rocks and the Gap site is 42 mi (68 km) south of Marathon, Texas, along U.S. Cretaceus cover (predominantly limestone) were involved in 385 (Fig. 1). The main outcrop is a prominent peak 0.5 mi (0.8 oblique overthrusting during Laramide left-slip transgression, lokm) east of the highway that can be reached easily by walking up tally creating a positive flower structure. Right-slip transtensional an arroyo into the hills (Fig. 2). Beware of cactus! Permission to faulting of the present cycle of Basin and Range deformation is walk off road should first be obtained at Persimmon Gap Ranger evident via downdropped fault blocks. The geologic history of the station 0.2 mi (0.3 km) south of the outcrop. The park has a region is dominated by repeated movements of basement-rooted nominal entrance fee. northwest-trending faults.
Classic “Kansas” cyclothems
Authors: Heckel Philip H. 
Published: November 2007

Abstract
This quadruple site (Fig. 1) illustrates typical examples of Kansas cyclothems of Pennsylvanian age.
Site 10: Iola and Wyandotte cyclothems (Figs. 2, 6). I-435 exit at Holliday Road, NE¼NW¼, Sec.6, T.12S., R.24E., Ed-wardsville 7½-minute Quadrangle, Johnson County, Kansas.
The best way to get to this section is to proceed south on I-435 from Kansas 32, cross the Kansas River and take the Holli-day Road exit around to the right, pulling off to park on the shoulder before meeting Holliday Road. The lower part of this section (up to the lower Argentine) is easily accessible on the east side of this ramp road, the upper part is accessible on the west side of this road, but requires more careful climbing.
Site 11: Swope and Dennis cyclothems (Figs. 2, 7). U.S. 69 roadcut by Jingo, SW¼SE¼, Sec.31, T.l8S., R.25E., New Lancaster 7½-minute Quadrangle, Miami County, Kansas.
This section is exposed continuously along the east side of U.S. 69 and the north side of a gravel section-line road that crosses U.S. 69, 13 mi (21 km) south of Kansas 68 (Louisburg) exit and 6 mi (9.6 km) north of Kansas 135 (LaCygne) exit. Park along the section-line road east of U.S. 69.
Site 12: Plattsburg cyclothem (Figs. 2, 8). Kansas 47 Altoona lower roadcut, near NW corner, Sec. 17, T.29S., R.16E., Altoona 7½-minute Quadrangle, Wilson County, Kansas.
The Anacacho Limestone of southwest Texas
Authors: Rodgers R. W. 
Published: November 2007

Abstract
The Anacacho Limestone represents an anomaly in the Gulfian-age rocks of Texas. Like the Austin Chalk that it unconformably overlies, the Anacacho is a limestone in a section dominated by terrigenous elastics and mudrocks; unlike the Austin Chalk (which is extensive throughout the margin of the Gulf Basin), the Anacacho is a small carbonate bank that extends less than 96 mi (160 km) along an east-west trend on the flanks of the Uvalde Salient. The formation thins perceptibly to the east toward San Antonio, where it is replaced by rocks of the Taylor Group. The formation reaches its maximum thickness on the flanks of the Uvalde Salient, and terminates abruptly at the western edge of the Anacacho Mountains. West of this termination the Anacacho is replaced by the Upson and San Miguel Formations.
From the Nueces River, west of the Uvalde Salient, westward to the Anacacho Mountains, the limestone outcrop is continuous for approximately 28 mi (46 km). The width of the outcrop varies from 2.4 mi (4 km) to 9 mi (15 km). East of the Uvalde Salient, outcrops of the Anacacho Limestone are discontinuous and scattered. Much of the section is either covered by alluvium or is lost along faults of the Balcones Fault Zone (Bureau of Economic Geology, 1974). This section, from Blanco Creek eastward to San Antonio, is approximately 60 mi (100 km) in length. However, outcrops in this section are limited in length from a few miles to several hundred feet. Exposures are mostly along
West Atchison Drift Section
Authors: Aber James S. 
Published: November 2007

Abstract
A series of long-studied exposures of glacial sediments is found immediately west of the city of Atchison, Atchison County, Kansas, along the south side of White Clay Creek in Sec. 2, 10, 1l, T.6S., R.20E. (Fig. 1). The stream cuts are readily accessible by foot from U.S. 59, which parallels the north side of White Clay Creek. It is advisable to ask local residents for permission to cross private property to reach the stream cuts.
Bunker Hill section of Upper Cretaceus rocks in Kansas
Authors: Hattin Donald E. , Twiss Page C. 
Published: November 2007

Abstract
The Bunker Hill section of the upper part of the Graneros Shale, Greenhorn Limestone, and of the lower part of the Carlile Shale is along the east side of Bunker Hill-Luray Road (Kansas FAS 47) about 4.5 mi (7.2 km) north of 1-70, along the center of the west line of Sec.18, T.13S., R.12W., Russell County, Kansas (Fig. 1). The top of the section is at the intersection with the unpaved side road to the east at an elevation of 1,790 ft (546 m); the base of the section is about 0.5 mi (0.8 km) north at an elevation of about 1,700 ft (518 m). Safest parking is on the side road near the top of the section (Fig. 1T).
Vehicles traveling on 1-70 should exit at the Bunker Hill exit (exit 193) and travel 4.5 mi (7.2 km) north through Bunker Hill to Sec. 18. The Bunker Hill exit is about 9 mi (14 km) east of Russell.
Rocktown channel in Dakota Formation of central Kansas
Authors: Twiss Page C. 
Published: November 2007

Abstract
The Rocktown channel sandstone of the Upper Dakota Formation is exposed on both sides of a road cut on Kansas 232, about 4.1 mi (6.6 km) north of 1-70 in the NW¼SE¼ Sec.19, T.12S., R.10W., Lincoln County, Kansas (Fig. 1). Vehicles traveling on 1-70 should exit at the Wilson and Wilson Reservoir exit (exit 206) and travel north on Kansas 232 toward Wilson Reservoir.
Ogallala Formation (Miocene), western Kansas
Authors: Gutentag Edwin D. 
Published: November 2007

Abstract
The area in the vicinity of Lake Scott State Park, Scott County, Kansas (Fig. 1), contains excellent outcrops of the Ogal-lala Formation. One of the best vertically continuous exposures is in the west side of the roadcut at the ridge called Devils Backbone, which is located in the NW¼, NE¼, Sec.25, T.16S., R.32W. This section is described in Table 1 and diagrammatically sketched in Figure 2.
Mine 19 geologic section, Pittsburg and Midway Coal Mining Company, Cherokee County, Kansas
Authors: Brady Lawrence L. 
Published: November 2007

Abstract
This site is an abandoned strip mine just south of West Mineral in northwest Cherokee County, in extreme southeastern Kansas. It can be reached most easily by traveling 5 mi (8 km) west from Kansas 7 on Kansas 102 to West Mineral and following local roads to the exposures shown in Figure 1.
Evaporates and red beds in Roman Nose State Park, northwest Oklahoma
Authors: Johnson Kenneth S. 
Published: November 2007

Abstract
Roman Nose State Park comprises 540 acres (219 hectares) of public lands where layers of Permian gypsum, dolomite, and shale are well exposed and where fresh water flows from three natural springs. The site is in the central part of Blaine County, northwestern Oklahoma (Fig. 1), located about 6 mi (10 km) north of Watonga, in Secs. 23 and 24, T.17N., R.12W. The park allows free access at all times and provides picnic and camping facilities; the park also contains a resort lodge, meals, and cottages. For information and access to springs and other areas partially closed during winter months (October 1 till early April), contact the Park Superintendent, Roman Nose State Park, Route 1, Box 2-2, Watonga, OK 73772 (telephone: 405/623-4215). The area is on the Watonga Lake 7½-minute Quadrangle.
Carbonate platform facies of the Morrowan Series (Lower Pennsylvanian), northeastern Oklahoma and northwestern Arkansas
Authors: Sutherland Patrick K. , Manger Walter L. 
Published: November 2007

Abstract
The localities described here form a transect from the Arkansas River, near Webbers Falls, Muskogee County, eastern Oklahoma, eastward to the Oklahoma/Arkansas boundary area near Evansville, Arkansas (Fig. 1). Detailed location data for each stop on the transect are given in the text.
Some aspects of the geology of Zodletone Mountain, southwestern Oklahoma
Authors: Donovan R.N. , Younger P. , Ditzell C. 
Published: November 2007

Abstract
Zodletone Mountain, a 250-ft-high (76 m) eminence in Kiowa County, southern Oklahoma, constitutes the northernmost member of the Slick Hills Range and rises 1,649 ft (500 m) above sea level (SW¼SW¼ Sec.9, T.6N., R.14W. Saddle Mountain 15-minute Quadrangle, Oklahoma). The best approach to the mountain is by following Oklahoma 58 south from Carnegie for 7 mi (11 km). At this point turn west along an unpaved section road for 3 mi (4.8 km), then south for 0.5 mi (800 m) to a white two-storied farmhouse, which is the home of Mr. Don Trobe (Fig. 1). Obtain permission to visit here. (Mr. Trobe, like everyone else hereabouts, has been very supportive of geologists. However, no smoking and no litter, please.) About 0.5 mi (0.8 km) south of Mr. Trobe—s home, turn west along another section road and drive 1.7 mi (2.7 km) to a silver gate at SE¼SW¼Sec.16, T.6N., R.14W. From here a fair-weather track runs north to the northeast side of Zodletone Mountain. Follow this track to its termination, park, and walk (but beware of rattlesnakes).
Max Meadows tectonic breccia at Pepper, Virginia
Authors: Schultz Arthur P. 
Published: November 2007

Abstract
Outcrops of extensive Max Meadows tectonic breccia are along the bluffs overlooking New River at Pepper, Virginia (Fig. 1). A few feet (m) northeast of the New River bridge on Virginia 114 turn north into a dirt road. Parkin the wide area just onto the dirt road and do not block the driveway to the private house. Do not drive to the outcrops on the dirt road which is a railroad right of way. Walk northeast about 1,000 ft (300 m) to the railroad tracks along the dirt road.
Chestnut Ridge fenster
Authors: Milici Robert C. 
Published: November 2007

Abstract
The Chestnut Ridge fenster area is located southeast of Ewing, Lee County, Virginia, in parts of the Coleman Gap, Ewing and Back Valley 7½-minute Quadrangles (Fig. 1). From Ewing, Virginia, proceed northeast 1.7 mi (2.7 km) on U.S. 58, turn right on Lee County road 744; proceed 1.1 mi (1.8 km) toroad fork, take right fork. (Route has been on rocks of the Knox Group; outcrops of the Maynardville Formation are exposed on left side of road 0.7 mi [1.1 km] south of road fork.) The fenster is exposed in the road and adajcent fields 1.0 mi (1.6 km) south of the road fork 0.3 mi (0.5 km) beyond the Maynardville Formation exposure.
Thorn Hill
Authors: Byerly Don W. , Walker K. R. , Diehl W. W. , Ghazizadeh M. , Johnson R. E. , Lutz C. T. , Schoner A. K. , Simmons W. A. , Simonson J.C.B. , Weber L. J. , Wedekind J. E. 
Published: November 2007

Abstract
The “Thorn Hill Section” is an amazingly complete and well exposed section of rocks that has served at least four generations of geologists as a reference for early Cambrian through early Carboniferous stratigraphy of the Southern Appalachians. Eastward from War Ridge along 8.8 mi (14 km) of U.S.25-E, across Clinch Mountain to Poor Valley Ridge, Grainger County, Tennessee, virtually every unit between the Rome and the Grainger formations in the Southern Appalachians is exposed in the 10,912 ft (3,326 m) thick sectio (Fig. 1). The section is bounded by two major thrust faults-the Copper Creekfault and the Saltville fault; the Rome Formation is the hanging wall forboth faults. Most of the section is embraced by the Avondale, 7½-minute topographic quadrangle with the remainder on the Dutch Valley, 7½-minute Quadrangle. The stratigraphic descriptions given here are synopses from Walker (1985). The stratigraphy here represents a westward thinning edge of a thick wedge dof Paleozoic sedimentary rocks whose history is recorded in three stratigraphic sequences bounded by unconformities of regional extent (Fig. 2). Sequence I embraces Cambrian through Early Ordovician, Sequence II the middle Ordovician through Early Devonian, and Sequence III Late Devonian through Early Mississippian.
The stratigraphic descriptions given here are synopses from Walker (1985). The stratigraphy here represents a westward thinning edge of a thick wedge of Paleozoic sedimentary rocks whose history is recorded in three stratigraphic sequences bounded by unconformities of regional extent (Fig. 2). Sequence I embraces Cambrian through Early Ordovician, Sequence II the middle Ordovician through Early
Saltville fault at Sharp Gap, Knoxville, Tennessee
Authors: Hatcher Robert D. 
Published: November 2007

Abstract
Sharp Gap is located on the north side of Frontage Road parallel to I-275 in Sharp Gap, which passes through Sharp Ridge, Knoxville, Tennessee (Fig. 1). It also includes exposure on the south side of Sharp Gap at road level off the side of I-275, Knox County, Tennessee, Knoxville and Fountain City 7½-minute Quadrangles, Tennessee (Cattermole, 1958, 1966).
Middle Ordovician shelf-edge skeletal sand-bank, organic build-ups, and quartz-sand-waves of the Holston and Chapman Ridge Formations near Knoxville, Tennessee
Authors: Walker Kenneth R. 
Published: November 2007

Abstract
This set of three outcrops is located south of the city of Knoxville, on the east side of Alcoa Highway (U.S. 129) one mi (1.6 km) south of the James E. Karnes Bridge over the Tennessee River (Fort Loudon Lake). The northernmost of the three outcrops is directly across Alcoa Highway from the Naval Reserve Station. The locality is in the southern part of the Knoxville 7½-minute Quadrangle (Fig. 1). The site is easily accessible, although Alcoa Highway is heavily traveled, and you are cautioned to cross the highway with great care. Parking is available on the east side of the highway just south of the Naval Reserve Station.
The Coosa deformed belt, thin imbricate thrust slices in the Appalachian fold-thrust belt in Alabama
Authors: Thomas William A. , Drahovzal James A. 
Published: November 2007

Abstract
A deep road cut on Alabama 77 (sec. 29, T.14S., R.6E.) near Ohatchee, Calhoun County, Alabama (Fig. 1), provides an exceptionally good view of imbricate thrust faults in the frontal tier of the Coosa deformed belt.
Sequatchie anticline, the northwesternmost structure of the Appalachian fold-thrust belt in Alabama
Authors: Thomas William A. 
Published: November 2007

Abstract
Two stops at Blount Springs, Blount County, Alabama (Fig. 1), provide traverses of parts of the Sequatchie anticline on the Blount Springs culmination. Blount Springs is on U.S. 31 approximately 4 mi (6 km) east of I-65. Interchange 287 on I-65 has only a northbound exit and a southbound entrance connecting with U.S. 31. Interchange 289 (north of Interchange 287 at U.S. 31) on I-65 has exits and entrances both northbound and southbound, and provides access to Blount Springs via Blount County Road 5.