bluuebunny/crossref_metadata_2025_split huggingface dataset:
Geology of the Buffalo River Valley in the vicinity of U.S. 65, Arkansas Ozarks
Authors: Craig William W. 
Published: November 2007

Abstract
U.S. 65 is a major north-south artery across Arkansas. In north-central Arkansas it traverses the Ozark Plateau Province, which represents a stable Paleozoic platform located on the southwest flank of the Ozark Dome and north of the Ouachita trough. In Searcy County the highway crosses the deeply incised valley of the Buffalo River (Fig. 1) about two-thirds of the distance from Harrison to Marshall.
Post-St. Peter Ordovician strata in the vicinity of Allison, Stone County, Arkansas
Authors: Craig William W. , Deliz Michael J. 
Published: November 2007

Abstract
Exposed at Allison are the Ordovician St. Peter Sandstone, Joachim Dolomite, Plattin, Kimmswick, and Fernvale Limestones, and Cason Shale, as well as the Mississippian Boone Formation. A geologic map of the vicinity of Allison is in McFarland and others (1979). The Allison section, along with related exposures, is included in Craig and others (1984). The outcrop consists of two obvious, closely spaced roadcuts, referred to by local geologists as Allison South and Allison West (Fig. 1). Allison South is on Arkansas 9, approximately 4 mi (6 km) north of Mountain View. Allison West is on Arkansas 14, approximately 0.5 mi (0.8 km) west of its junction with Arkansas 9, between the small community of Allison and the entrance to Blanchard Spring Caverns. The roadcuts are in Sec. 14 and 10, T.15N., R.11W. of the Sylamore and Fifty Six 7½-minute Quadrangles, respectively.
Both Allison localities are easily accessible. Neither Arkansas 9 nor 14 is heavily traveled. Ample shoulder space makes these locations ideal for relatively large groups. Parking at Allison South is better on the shoulder west of the highway. A turnout opposite Allison West allows convenient parking there. Allison South provides a nearly complete exposure from uppermost St. Peter Sandstone through Plattin Limestone. Higher rocks are better viewed at Allison West, which exhibits a complete section from uppermost Plattin into the lower part of the Boone Formation.
Crowley’s Ridge, Arkansas
Authors: Guccione M. J. , Prior W. L. , Rutledge E. M. 
Published: November 2007

Abstract
Crowley’s Ridge is an erosional remnant of unconsolidated Tertiary clay, silt, sand, and lignite capped by Pliocene- Pleistocene gravel, sand, and clay, and middle-to-late Pleistocene loess (Haley, 1976). Located in eastern Arkansas and southeast Missouri, Crowley’s Ridge is no more than 11 mi (18 km) wide, but it extends for 186 mi (300 km) from Campbell, Missouri, to Helena, Arkansas (Fig. 1). The ridge stands 100 to 200 ft (30 to 60 m) higher than the adjoining Eastern and Western Lowlands.
Crowley’s Ridge was a divide formed during the Pleistocene, as ancestors of the Mississippi River to the west and the Ohio River to the east of the Ridge eroded Coastal Plain sediments (Call, 189 1; Fisk, 1944) (Fig. 2). At that time the two rivers joined near Simmesport, Louisiana, 404 mi (650 km) south of where they join today. Abundant glacial outwash and a rising sea level contributed to the aggravation of the ancestral Mississippi and Ohio Rivers, causing a decrease in their gradients. This decrease in gradient and tectonic activity along the New Madrid seismic zone may have caused the eastward shift of the Mississippi River, culminating in the cutting of the present channel through the divide at Thebes Gap. Today the Mississippi River joins the Ohio River near Cairo, Illinois, and flows on the east side of the ridge.
Atokan stratigraphy of the Cherry Bend area, north western Arkansas
Authors: Harris Gary D. , Ramsey Dean A. , Zachry Doy L. 
Published: November 2007

Abstract
The Cherry Bend area is astride Arkansas 23 approximately 5 mi (8 km) south of Brashears, Arkansas (Fig. 1, inset), and is immediately north of the east-trending Cass Fault-Monocline System of the northern margin of the Arkoma Basin. Access to the various stops in the Cherry Bend area is from well-maintained forest service roads, and from Arkansas 23, as well as from the Ozark Highland Trail that transects the area from west to east (Fig. 1). The area is contained entirely within the Cass 7½-minute Quadrangle.
I-430 bypass, Little Rock, Arkansas
Authors: McFarland J. D. 
Published: November 2007

Abstract
The 1-430 bypass around the west end of Little Rock, Arkansas, offers a unique section of Paleozoic age rocks demonstrating the various facies and structural styles in the eastern Ouachita Mountains (Stone and McFarland, 198 1). The sections are easy to reach; just drive to Little Rock, Arkansas, on the interstate system and follow the signs to 1-430. The site descriptions are arranged from north to south, starting about 0.8 mi (1.3 km) south of the 1-430 bridge over the Arkansas River.
Igneous rocks at Granite Mountain and Magnet Cove, Arkansas
Authors: Howard J. Michael , Steele Kenneth F. 
Published: November 2007

Abstract
The Granite Mountain area (Fig. 1) is located to the south of Little Rock, Arkansas, just south of the interchange between U.S. 65/167 and 1-30/630. The exposures at Magnet Cove are located along or near Arkansas 51 west of 1-30, about 40 miles southwest of Little Rock.
The Crouse Limestone in north-central Kansas; Lateral changes and paleoecological analysis
Authors: West R. R. , Twiss P. C. 
Published: November 2007

Abstract
Exposures of the Crouse Limestone along 1-70 south and east of Manhattan, Kansas (Fig. 1), illustrate the stratigraphy, structural geology, palaeoecology, and cyclic sedimentation in the Permian rocks of eastern Kansas. This text provides details of four exposures (between mileposts 319 and 305) that emphasize the interrelationships among these four areas of geology.
Ogallala and post-Ogallala sediments of the Southern High Plains, Blanco Canyon and Mt. Blanco, Texas
Authors: Dolliver Paul N. , Holliday Vance T. 
Published: November 2007

Abstract
Blanco Canyon and Mount Blanco are located along the eastern Caprock Escarpment of the Southern High Plains (Llano Estacado) in the Texas Panhandle near Crosbyton, Texas. The Blanco Canyon exposures are along U.S. 82 where it crosses lower Blanco Canyon east of Crosbyton (Fig. 1). Within a distance of 5.5 mi (8.9 km), the highway descends from the High Plains through the Bridwell and Couch Formations (Ogallala Group) to Triassic red beds before climbing back onto the High Plains surface. The route passes near the Bridwell and Couch type sections and is flanked by several excellent roadside exposures. Outcrops at four Blanco Canyon localities are discussed in this chapter. Collectively, they document the buildup and subsequent dissection of the Southern High Plains since late Miocene time.
Mt. Blanco can be reached by traveling north from Crosbyton on Farm Road 651 across the High Plains surface (Backwater Draw Formation). At 7.8 mi (12.5 km) the road descends into Blanco Canyon. Below the escarpment the highway crosses the mouth of Crawfish Creek, a major reentrant of Blanco Canyon. As the road descends the side of the canyon, the white beds of the Blanco Formation are apparent to the left and right just below the reddish sands of the Backwater Draw Formation. After descending into the canyon, turn left (west) on Farm Road 193 and drive 0.7 mi (1.1 km) to Mt. Blanco, which is the conical erosional remnant on the south side of the road.
Middle and Upper Pennsylvanian (Atokan-Missourian) strata in the Colorado River Valley of Central Texas
Authors: Grayson Robert C. , Trite E. L. “Jack” 
Published: November 2007

Abstract
The Middle and Upper Pennsylvanian stratigraphic sequence of Central Texas is exposed in a triangular shaped region that is bisected by the Colorado River (Fig. 1). This succession of strata (Fig. 2) is illustrated in this double-site guide. Site 78 begins in San Saba County near Bend, Texas, where exposures of the Marble Falls Limestone, Smithwick Shale, and lower “Strawn” Group are available for study. Three additional localities in San Saba and Mills counties permit special emphasis on the depositional character of the lower “Strawn” Group. The upper Strawn Group, Site 79, is seen along a transect across the outcrop belt in San Saba and McCulloch Counties. Single localities at opposite ends of the outcrop belt in San Saba and Brown Counties (Fig. 1) further document the various lithologies and stratigraphic relationships of the upper unit.
Beattie Limestone (Lower Permian) of eastern Kansas
Authors: Twiss Page C. 
Published: November 2007

Abstract
The Beattie cyclothem (site 8) is exposed on the north side of a road cut about 325 ft (100 m) west of milepost 317 on 1-70 in the center of NE¼, Sec.26, T.11S., R.8E., Riley County, Kansas (Fig. 1). If traveling eastward, continue to exit 318, pass under 1-70, and return to the road cut (Kansas law prohibits pedestrians from crossing divided highways). Vehicles should be parked off the pavement, and passengers should exit vehicles on the north side. Keep as far as possible from the traffic lane while examining the rocks.
The Cottonwood Limestone Member of the Beattie Limestone (site 9) is exposed on the north side of a road cut at milepost 272 on U.S. 54 about 0.3 mi (0.5 km) east of the Butler County line. The outcrop is near the north edge of SE¼, SW¼, Sec.3, T.26S., R.8E., Greenwood County, Kansas (Fig. 2). Vehicles should be parked on the south side of the highway where the old road enters the present highway.
The middle Comanchean section of Central Texas
Authors: Amsbury David L. 
Published: November 2007

Abstract
The text describes outcrops of Comanchean strata around Lake Travis on the Colorado River between Austin and Marble Falls in central Texas (Fig. 1). The exposures selected are readily accessible and can provide a good understanding of the vertical sequence of Upper Aptian through Middle Albian rock types. Appreciation of the three-dimensional relationships will require study of the listed publications. Many good exposures occur on private property within the region, but most are not indicated in the guide. The geologist in central Texas is well advised to refrain from crossing any fences for any reason without prior permission from the landowner (and land manager, if appropriate).
The lower Tertiary of the Texas Gulf Coast
Authors: Yancey Thomas E. , Yancey Elizabeth S. 
Published: November 2007

Abstract
The lower Tertiary section in the western Gulf Coast is most complete and best exposed in the bluffs of the Brazes River Valley (Figs. 1 and 2), and has received the most study of any area in the state. The low rolling hills of this region provide limited outcrops, so most good exposures are confined to high banks along the Brazes River. Strata dip toward the Gulf of Mexico at uniformly low dips, and exposures gradually shift upsection as one travels downriver. The regular progression upsection continues to the area of Navasota and Hempstead, where Quaternary sediments of the flat-lying coastal plain lap onto the youngest (Miocene age) of the more steeply dipping Tertiary formations. The Brazes Valley was one of the more heavily traveled routes by settlers and explorers, and the Stone City locality (site of the King’s Highway [El Camino Real or Old Spanish Road—OSR] crossing of the Brazes River) was the source of material for the first study of Texas fossils.
Precambrian and Paleozoic stratigraphy; Franklin Mountains, west Texas
Authors: LeMone David V. 
Published: November 2007

Abstract
The Franklin Mountains are located in far West Texas (ElPaso County) and southernmost central New Mexico (Dons Ana County). The range, when including the North Franklin Mountains (north of Anthony Gap), is 23 mi (38 km) long and less than 5 mi (8 km) wide (Fig. 1). It consists of a linear series of north–south-trending, westward-tilted fault blocks, which are bounded on the east and west by major normal faults. Gravity slides are common throughout the range. The mountains are reasonable examples of the basin-and-range structural and physiographic type. The structure is distinctly different from the thrusted (autochthon and three allochthons) Cretaceus sequence of the northern Chihuahuatrough of the Sierra de Juarez to the south in Mexico. The Texas lineament, the major structural feature separating these disparate northern and southern structural styles, if it exists, would pass through downtown El Paso. Access to the area is by 1-10. Three localities are suggested for examination (Fig. 1). Localities 1 and 2 are on paved, public thoroughfares. Locality 3 (Vinton Canyon) maybe reached from 1-10 at Westway, approximately 3 mi (4.8 km) south of the Texas-New Mexico line, byproceeding eastward on a dirt track toward the mountains. A high-clearance vehicle is required.
The southern Guadalupe Mountains, Texas; Permian stratigraphy and Great Plains/Basin and Range structural transition
Authors: McKnight Cleavy L. 
Published: November 2007

Abstract
The Guadalupe Mountains, easternmost of the block-faulted ranges of the Basin and Range at this latitude, expose a classic section of Permian shelf and basin carbonates and elastics (King, 1942, 1948). In a series of panoramic views and roadcuts the southern Guadalupe Mountains in Culberson and Hudspeth counties, Texas, display both the Permian stratigraphic transition of shelf elastics and evaporates to shelf-margin carbonate buildups to basinal elastics and the modern physiographic/structural transition from the relatively undisturbed, flat-lying sedimentary strata of the Great Plains to the tilted and block-faulted rocks of the Basin and Range. The exposures are all located along U.S. 62-180. Stop 1 is located 43 mi (69 km) southwest of Carlsbad, New Mexico; Stop 4, the final locality, is located 37 mi (59 km) farther west, or 96 mi (154 km) east of El Paso, Texas. The immediate field area is shown in Figure 1. The regional geography is shown on the Van Horn, Texas (1975), and Carlsbad, New Mexico (1972), 10 x 2° topographic sheets; geographic place names not shown in Figure 1 may be found on these two maps. The route traverses the South Rector Canyon (1973), Independence Spring (1973), Guadalupe Peak (1973), Guadalupe Pass (1973), Patterson Hills (1973), and Linda Lake South (provisional, 1984) 7½-minute Quadrangles, all in Texas.
Lower Cretaceous of western Trans-Pecos Texas
Authors: Amsbury David L. , Reaser Donald F. 
Published: November 2007

Abstract
The area is accessible from 1-10, U.S. 90, and (from Big Bend National Park) Texas 170. Outcrops of Lower Cretaceous rocks occur along public roads near Kent; south of Sierra Blanca in the Quitman Mountains; southwest of Marfa and north of the Chinati Mountains; and south of Shafter (Fig. 1).
The Davis Mountains volcanic field, west Texas
Authors: Parker Don F. 
Published: November 2007

Abstract
The Davis Mountains are located south of the junction of 1-10 and 1-20 and northwest of Alpine, predominantly in Jeff Davis County, southwestern Texas. The 14 field localities described here are keyed to the schematic cross sections of Figure 1. The field localities vary from roadcut exposures to hillside exposures to scenic panoramas; all were chosen to elucidate important features of Davis Mountains geology. A brief description of the location, the rock units involved, and chief references are given for each locality. K-Ar ages on Figure 1 were recalculated from Parker and McDowell (1979), using new standard decay constants (Steiger and Jager, 1977).
Dikes in Big Bend National Park; Petrologic and tectonic significance
Authors: Price Jonathan G. , Henry Christopher D. 
Published: November 2007

Abstract
Dikes in Big Bend National Park illustrate the petrologic variety and tectonic setting of Tertiary magmatism in Trans-Pecos Texas. Most igneous activity occurred between two major episodes in the tectonic history of western North America: (1) Late Cretaceus to early Eocene Laramide compression and (2) late Oligocene to recent Basin and Range extension. Volumetrically minor magmatism occurred during the initial stage of Basin and Range extension and perhaps during the final stage of Laramide deformation.
The general geology of the park, including aspects of stratigraphy, structure, petrology, and geomorphology, is best described in the treatise by Maxwell and others ( 1967). The 1:62,500-scale geologic map in Maxwell and others’ (1967) volume is also available at many stores in the Big Bend region as part of a nontechnical geologic guide to Big Bend by Maxwell (1968). The 1:250,000-scale geologic map by Barnes (1979) covers the southern part of the Trans–Pecos region. A field trip guidebook by Maxwell and Dietrich (1972) complements these publications. More recent studies have added considerably to our understanding of the tectonics, volcanic stratigraphy, and petrology of the region. Research results are summarized in guidebooks edited by Dickerson and Hoffer (1980), Dickerson and Muehlberger (1985), and Price and others (1986). In addition, details of the tectonic and magmatic history of the Trans–Pecos region are provided by Henry and Price (1984, 1985, 1986), Price and Henry (1984), and Price and others (1987).
This chapter describes localities for examining dikes in Big Bend National Park (Fig. 1). These dikes represent
Lower Cretaceus Kiowa Formation; The eastern margin of the Western Interior Seaway
Authors: Scott Robert W. 
Published: November 2007

Abstract
The Kiowa Formation is exposed discontinuously along the shores of Kanopolis Reservoir in central Kansas. This reservoir was formed by the damming of the Smoky River in Ellsworth County about 20 mi (32 km) southwest of Salina. One of the best exposures is about 660 ft (200 m) southwest of the dam control tower along the shore (NE¼, Sec.3, T.17S., R.6W.; 97°58′ W., 38°36—30—N.; Crawford 1964 USGS topographic sheet) (Fig. 1). The outcrop is accessible by a short hike west of the road leading across the dam. The condition of the exposure depends on the water level and varies from time to time. A similar section is exposed along the eastern bluff in the second bay west of the state campground. It is accessible by walking northwest a few hundred meters from the road (C. NE¼, Sec.4, T.17S., R.6W.;97°59—W., 38°36—24—N.). The unfossiliferous lower part of the section is partly exposed on private land east of the dam (SW¼, Sec.l, T.17S., R.6W.;97°56—36’W., 38°36—24’N.)
Plio-Pleistocene rocks, Borchers Badlands, Meade County, south western Kansas
Authors: Zakrzewski Richard J. 
Published: November 2007

Abstract
The Borchers Badlands, hereafter referred to as the badlands, are located in the south-central part of Meade County, Kansas, approximately 9 mi (14.4 km) south-southwest of Meade, the county seat (Fig. 1). This area is part of the transition zone between the High Plains and the Plains Border provinces. Meade is at the junction of U.S. 54 and 160 and Kansas 23. The latter highway bisects the badlands into a north half (Section 4) and a south half (Section 3). The badlands are located in Sec. 16; a small portion of the SE¼ of Sec. 17; the east half of Sec. 20 and the west half of Sec. 21, T33S., R.28W. (Fig. 2), an area of approximately 2 mi2 (5.2 km2) (Lake Larabee and Irish Flats NE7½-minute Quadrangles). The western boundary is Crooked Creek, a fault-controlled stream. The eastern boundary is the undissected upland area.
The Meers fault scarp, southwestern Oklahoma
Authors: Donovan R.N. 
Published: November 2007

Abstract
The Meers fault scarp trends ESE-WNW along the northern edge of the Meers Valley in Commanche County, southwestern Oklahoma (Fig. 1 ). The impressively straight scarp can be traced for 16 mi (26 km). The southeastern two-thirds of the scarp intends across land that is under relatively intensive agricultural use, and the northwestern third extends across hilly open range. This land usage reflects the underlying Permian bedrock shales to the southeast and conglomerates to the northwest. The most visually impressive and instructive lengths of scarp are developed in the conglomerate terrain. Access procedure to a convenient length of the scarp in this terrain is as follows. First, contact Mr. Charlie Bob Oliver, manager of the Kimbell Ranch. The ranch house is located in Blue Creek Canyon on Oklahoma 58. Mr. Oliver has been closely involved in recent work on the fault and, if notified in advance, can make a key to the ranch tracks available. Oklahoma 58 must be followed south of Stumbling Bear Pass to a county road (Fig. 2). This road should then be taken for just over 1 mi ( 1.6 km) west to a group of houses north of the road. At this point a decision must be made with respect to the condition of a ranch track which trends north by the houses. This road is impassable for most vehicles after a rain (the alternative is a walk of about 1.5 mi; 2.4 km). The track is followed north for about 0.5 mi (0.8 km)
Deltaic facies of the Hartshorne Sandstone in the Arkoma Basin, Arkansas-Oklahoma border
Authors: Houseknecht David W. 
Published: November 2007

Abstract
Sedimentary facies deposited in channel and interchannel positions within an actively prograding, river-dominated delta are illustrated at two localities near the Arkansas-Oklahoma border south of Fort Smith, Arkansas.
Locality 1 (94°17—20"W.; 35°11'41—N.; Greenwood, Arkansas, Quadrangle) is a distinctive, terraced roadcut on U.S. 71, approximately 12 mi (20 km) south of Fort Smith (Fig. 1). The Hartshorne Sandstone dips steeply north (nearly vertical) along the north limb of the Washburn anticline (Fig. 2).
Locality 2 (94°31—20W.; 35°10—30"N.; Spiro, Oklahoma, Quadrangle) is a roadcut on old Oklahoma 112, approximately 8 mi (12 km) west of Hackett, Arkansas (Fig. 1). The Hartshorne Sandstone dips 15° southward along the southern limb of the Backbone anticline (Fig. 2).
Appalachian Valley and Ridge to Appalachian Plateau transition zone in southwestern Virginia and eastern West Virginia
Authors: Whisonant Robert C. , Schultz Arthur P. 
Published: November 2007

Abstract
The Appalachian Valley and Ridge to Appalachian Plateau transition is exposed in a series of road cuts located in Giles County, Virginia, and Mercer County, West Virginia, and include portions of the Narrows, Oakvale, Lerona, and Peterstown 7½-minute Quadrangles (Fig. 1). The exposures may be reached via U.S. 460 approximately 15 mi (24 km) east of Princeton, West Virginia, or 2 mi (3 km) north of Narrows, Virginia.
The Upper Ordovician Fredericktown Section, Nelson County, Kentucky
Authors: Noger Martin C. 
Published: November 2007

Abstract
The Fredericktown Section is in Nelson County, Kentucky, in the southwestern quarter of the Maud 7½-minute quadrangle (Peterson, 1972) in a roadcut along the southwestern side of U.S.150, 4.5 miles (7.2 km) east of the Bluegrass Parkway (Fig. 1).
Flood-tidal deltas and related back barrier systems
Authors: Haas Christopher A. , Gastaldo Robert A. 
Published: November 2007

Abstract
Two outcrops of the Bremen Sandstone are located on or near River Highway, 2.4 mi (3.9 km) north of Alabama 69, in Sec.l, T.13S, R.6W, and Sec.6, T.13S, R.5W, Walker County, Alabama, on the Lewis Smith Lake Dam 7½-minute Quadrangle.
Pottsville Formation in Alabama
Authors: Rheams Lawrence J. , Benson D. Joe 
Published: November 2007

Abstract
Six exposures of the Early Pennsylvanian Pottsville Formation in the Warrior coal field of Alabama can be seen along I-65 starting just north of Birmingham, Alabama and ending about 36 mi (60 km) farther to the north (Fig. 1). The stops illustrate the stratigraphy, structure, and depositional environments of a part of the Pottsville interval in the Warrior coal field.