bluuebunny/crossref_metadata_2025 huggingface dataset:
The Indiana Dunes area, northwestern Indiana
Authors: Hill John R.
Published: November 2007

The area designated as the Indiana Dunes is in Lake, Porter, and LaPorte Counties in northwestern Indiana. Including roughly 45 mi (72 km) of shoreline at thesouthern tip of Lake Michigan, the dunes area is replete with numerous well-developedgeomorphic features that formed in response to the final stages of the Lake Michigan Lobe of the Laurentide Ice Sheet. Attractingsuch skilled researchers as T. C. Chamberlain, FrankLeverett, William Alden, Frank Taylor, Jack Hough, and J Harlen Bretz, southern Lake Michigan and environs have yielded a wealth ofinformation about the formative stages of the Great Lakes as well as glaciological mechanisms responsible for their genesis. Thedunes area of Indiana is of particular interest because of the wide variety of dune forms, well-preserved glacial-lake terraces, andimpressive topography of the Valparaiso Moraine that remain relatively unspoiled.

Magnificent examples of blowout dunes, first described by George Babcock Cressey in 1928, can be seen all along the beach of the Indiana Dunes State Park. Access to the park is by Indiana 49 (Fig.1). Numerous well-marked trails traverse the 2, 100-acre (840 ha) park, providing ready access to the foredune complex of the modern beach as well as the interdunal and back-dune areas that formed during the several stages of glacial Lake Chicago.

The Indiana Dunes National Lakeshore affords numerous access points to, perhaps, the greatest variety of geologic features within the Lake Michigan Basin. Interested persons should stop at the visitor center, which is at the intersection of U.S. 12 and Kemil
The Kentland Dome, Indiana
Authors: Gutschick Raymond C.
Published: November 2007

Abstarct

The Kentland Dome is an enigmatic, thought-provoking, structurally complex anomaly, subsequently covered by glacial drift, in an area surrounded by normal, undisturbed, flay-lying Paleozoic strata. Rocks in thecore of the Kentland structure havebeen uplifted more than 2,000 ft (610 m), folded into a structural dome, and intricately disrupted by faulting. A significant portion of the Ordovician central core is revealed in the spectacular Kentland Quarry. One must see the quarry and its superb rock exposures that challenge the imagination to grasp the magnitude of the anomaly and complexities of its structural pattern.

The oldest quarries at Kentland (McKee and Means) date from more than 100 years ago. Since that time, generations of geologists, applying the scientific method to the exposures in the continually expanding quarry, have built a case history on the evolution of thought to the origin of this unusual structure. The problem has been, and remains, to explain this geometic jigsaw puzzle with respect to its spatial pattern, chronology of disruption, and genesis of deformational mechanics. For example, shatter cones and their orientations in the Kentland Quarry inspired Dietz (1947, 1972) to suggest a meteorite-impact origin simply because the cone apices point upward upon reconstruction of the strata to their normal, flat-lying position. Are Dietz, and other devotees of extraterrestrial origin, correct? Or are there plausible alternative endogenetic explanations?

References to significant developments of the quarries at Kentland and in thought on the origin of the structure can be found in various annual reports
The Lovers Leap section and related observations of multiple and cross-cutting glacial drifts in the Great Bend area, Indiana
Authors: Bleuer N. K. , Shaver Robert H.
Published: November 2007

Abstarct

The glacial geology of the area north of the Great Bend of the Wabash River in west-central Indiana (Fig.1), 1) illustrates important early developed principles regarding multiple continentalglaciation, the movements of adjoining ice lobes, and the interrelated deposits. Perhaps the first documentation of a lithologically definable till stratigraphy that is basic to interpretation of glacial movement and sedimentation throughout much of the Midwest was made in the Great Bend area. A half century after the first documentation was made, the till stratigraphy here would emerge as the regionally mappable sequence. Further, it would illustrate cross-cutting relationships of morainal ridges andthe interbedding of multiple-source deposits. Here, therefore, is a clear demonstration of how deposits first classified on the basis of surface morphology relate to those that are classifiable on a mappable, till-stratigraphy basis.

Four vantage points in the Great Bend area are particularly focal for illustration ofthe basic concepts that are addressed here.Foremost is the Lovers Leap section (also known historically as the Stone Creek section), which is exposed on the northwest side of Big Pine Creek, a Wabash River tributary, 4 mi (6.4 km) north of Williamsport, Warren County, Indiana, NW¼NW¼ NW¼Sec.23, T.22N., R.8W., Williamsport 7½-minute Quadrangle (Fig. 2d), 2D). Here well exposed are three superimposed tills and other drift materials that a pioneer of continental-glaciation theories, Thomas Chrowder Chamberlain, used to demonstrate his beliefs. In fact, our Figure 3 is taken from Chamberlin’s contribution to James Geike’s ( 1894) The Great Ice Age and was
Pennsylvanian and Permian rocks associated with the Humboldt Fault Zone in southeastern Nebraska
Authors: Burchett Raymond R.
Published: November 2007

This outcrop of Pennsylvanian and Permian rocks is along the east side of Nebraska 105 about 3 mi (5 km)south of Humboldt in Richardson County, Nebraska. It is located in the SW¼ Sec. 22 and NW¼ Sec. 27, T.2N., R.13E., as shown in Fig. 1, which reproduces a small part of the Humboldt SW 7½-minute Quadrangle. The rocks are exposed on public right-of-way in the road ditch eastof the highway and are easily accessible by foot.

Here is a good exposure of the contact between the Pennsylvanian and Permian rocks and also one of the best localities in Nebraska to observe steeply dippingrocks associated with the Humboldt Fault Zone. The exposure here is approximately 170 ft (51.8 m) thick. The dip is 17°E.
The Orangeville Rise and Lost River, Indiana
Authors: Powell Richard L.
Published: November 2007

The Orangeville Rise is the spring head of Lost River in the town of Orangeville in northwestern Orange County. The site is about 6 mi (9.6 km) northeast of French Lick and 9 mi (14.4 km)southwest of Mitchell. (See location in Fig. 1; also, the inset mapin Fig. 5 shows locations of other features mentioned here.) The Orangeville Rise is owned by the Nature Conservancy and is a National Natural Landmark registered by the U.S. National ParkService. The spring is the most accessible of several sites that arecommonly visited on field trips and are considered to be focalpoints that depict significant aspects of subterranean drainage in the Lost River basin. In addition to the Orangeville Rise, the other nearby sites singled out here are the Rise of Lost River, Tolliver Swallow Hole, and Wesley Chapel Gulf.

The Lost River drainage basin heads on the Mitchell Plain, a low limestone plateau developed on the westward-sloping vale of an east-facing cuesta. The dip of the strata is only slightly greaterthan the general slope of the plain. To the west, the Crawford Upland is a rugged hilly area separated from the Mitchell Plain bythe east-facing Chester Escarpment. Similar physiographic unitsto the south in Kentucky are the Mammoth Cave Plateau and the Pennyroyal Plateau separated by the Dripping Springs Escarpment.A few major streams flow in entrenched sinuous valleyswestward across the Mitchell Plain and the Crawford Upland,

Most of the eastern part of the Mitchell Plain is mantled with clay
The Chesterian section near Sulphur, Indiana
Authors: Horowitz Alan Stanley , Kelly Stuart M.
Published: November 2007

A remarkable exposure of early and middle chesterian (Late Mississippian) rocks is found at the junction of I-64 and Indiana 37 approximately 1 mi (1.5 km) north of Sulphur, Crawford County, Indiana (N½S½Sec.24,T.3S.,R.1W., Beechwood 7½-minute Quadrangle; Fig. 1). S me of the geological boundaries in the area are shown on the geologic maps prepared by Perry and Smith (1958, plate 2) and Gray and others (1970).

This site can be reached by exiting I-64 at its junction with Indiana 37 north from Tell City or south from IndianapolisBloomington, Bedford, or Paoli. Safe offroad vehicle parking on blacktop is present along Indiana 37 at its junction with all four interstate ramps. Examination of the upper part of the section requires the climbing of exposures that are revealed to best advantage in the northwestern road cuts.
Lake Erie
Authors: Carter Charles H.
Published: November 2007

Headlands Beach State Park is located adjacent to the mouth of the Grand River, and Gainesville Township Park islocated about 2 mi (3.2 km) east of the mouth of the Grand River; the sites are near the middle of the south shore of Lake Erie (Fig. 1). Each site can be reached from roads running north of Ohio 2 (a major, four-lane, divided highway): Headlands Beach from Ohio 44 that runs directly into the park at a distance of about 2.4 mi (3.8 km) from Ohio 2 and Gainesville Township Park from Ohio 535 to Hardy Road at a distance of about 2.1 mi (3.4 km) from Ohio 2. One can also follow a circuitous route-mostly Ohio 535 and 283-between the two sites (Fig. 1).

Buses can be driven to both sites. At Headlands Beach it easiest to park in the easternmost parking lot, then walk northwest through the dunes to the beach and shoreline, then northeast to the jetty, and then return south along the jetty. At Gainesville Township Park one can look at the observation point just beyond the east side of the park where the road (John Bailey Drive) has been cut off by erosion and then take a path at the western end of the park to reach the beach.
Hueston Woods State Park
Authors: Stewart David P. , Miller Barry B.
Published: November 2007

The exposure described in this report is located in Hueston Woods State Park, in Butler County, southwestern Ohio. It is southwest of Eaton, which is 7 mi (12 km) south of Interstate 70 on U.S. 127, and it is 25 mi (40 km) north of Cincinnati and 1–71 and I–75 (Fig. 1). The site (Doty’s Highbank) is located onthe east side of Four Mile Creek, 3 mi (5 km) north of Oxford (Oxford 7½-minute Quadrangle).

Access to the site is by Ohio 732 (Fig.2). Turn weston Park Road and continue for about 0.5 mi (0.8 km) to a junction, turn left (south), and follow this road until it crosses Four Mile Creek. Park southwest of the bridge, walk across the bridge, and follow the east side of the creek downstream 750 ft (230 m) to a high stream-cut exposure.
Copperas Mountain
Authors: Carlson Ernest H.
Published: November 2007

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

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

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

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

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

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

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

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

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).
Atoka Formation in the Lee Creek area, Arkansas
Authors: McFarland J. D.
Published: November 2007

The outcrops described here are found along Arkansas 220 in northern Crawford County. Start at the intersection of Arkansas 59 and 220. Drive north on Arkansas 220 for 0.1 mi (0.16 km) to Stop 1.
Blue Mountain Dam and Magazine Mountain, Arkansas
Authors: Cohoon Richard R. , Vere Victor K.
Published: November 2007

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

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

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

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

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

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

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

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

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

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

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

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

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
Mid-Tertiary and Pleistocene sections, Sotol Vista to Cerro Castellan, Big Bend National Park, southwestern Brewster County, Trans-Pecos Texas
Authors: Stevens James B.
Published: November 2007

Texas 118 becomes the main park road at the western entrance to Big Bend National Park, in southwestern Brewster County, Trans-Pecos Texas. The traverse lies along Ross Maxwell Appreciation Scenic Drive, which turns off the main park road 9.4 mi (15.1 km) east of this entrance, and provides principal access to the southwestern part of the park. The traverse begins at Sotol Vista (Fig. 1), a 0.3 mi (0.5 km) loop off the drive 8.5 mi (13.7 km) from the turn, and ends at the eastern base of Cerro Castellan 9.4 mi (15.1 km) to the southwest.

The traverse provides examples of the stratigraphy (Figs. 2,3) and structure on which many conclusions about the eastern part of an intraplate boundary are based. This traverse lies entirely within a national park; without the proper permits it is illegal to collect rocks, fossils, plants, or animals, and unwise to carry a rock hammer. Collecting permits should be arranged well in advance with the Resource Management Office, Big Bend National Park. It is also important to remember that this is desert country. There is no reliable supply of potable water along Ross Maxwell Appreciation Drive.
Late Quaternary geology of the Texas coastal plain
Authors: Morton Robert A.
Published: November 2007

Modem depositional environments prominently displayed along the northwestern Gulf of Mexico served as the first widely accepted sedimentary facies models that have successfully guided exploration and production of a variety of energy and nonfuel resources (petroleum, lignite, uranium, geothermal energy, construction aggregate, ground water). Because these industrial activities both required and provided a tremendous data base, the depositional environments of the gulf coast are among the best known anywhere. The following sections of the guidebook describe selected geological features that typify late Pleistocene and Holocene sediments of the Texas coastal plain and illustrate the diversity of associated depositional environments. The described sites represent a spectrum of transgressive and regressive sequences coexisting along a microtidal storm-dominated coast undergoing a significant reduction in sediment supply and a slight sea-level rise. Late Quarternary history. The Texas coastal plain is a broad, flat, depositional surface created by several rivers that eroded large volumes of sediment from remote areas of the state and adjacent mountainous regions and deposited the sediment as coalescing deltas in the Gulf of Mexico (Barton, 1930, Doering, 1935; Winker, 1979). It extends eastward and merges with the coastal plain of Louisiana, which has a similar morphology but a slightly different origin. Rather than being formed by several rivers and deltas of moderate size as was the Texas coast, the Louisiana coastal plain was mostly deposited by two large alluvial systems (Mississippi and Red rivers) that drained much of the continental interior.

Like present-day rivers, the load and discharge of these late
Carlton rhyolite and lower Paleozoic sedimentary rocks at Bally Mountain in the Slick Hills of southwestern Oklahoma
Authors: Donovan R.N. , Ragland D. , Cloyd K. , Bridges S. , Denisen R. E.
Published: November 2007

The Bally Mountain Range is located in eastern Kiowa County in southwestern Oklahoma (T.6N., R.14W.). The closest important road is Oklahoma 58 (Fig. 1). This road can be accessed from the H. E. Bailey Turnpike by taking the Medicine Park exit a few miles north of Lawton. Alternatively, the route can be joined from the north by taking the Hydro exit from 1-40. The easiest way of reaching the site is to proceed north on Oklahoma 58 for 3 mi (4.8 km) from its junction with Oklahoma 19, then turn west along a partly paved county road for 3 mi (4.8 km). Just before reaching the most prominent hill in view (which is Bally Mountain), turn right on an unpaved road and proceed north for a few hundred yards to the only inhabited house (on the west side of the road). This is the home of Mr. W. Hodges, the principal landowner in the area, where permission to visit the site should be sought. In common with several other landowners in the area, Mr. Hodges freely allows large parties of students access to his land on condition that they do not smoke or leave litter and that they close all gates, etc. His house is very conveniently situated; immediately to the west is the bulk of Bally Mountain, which is composed of Carlton Rhyolite. This hill is 1,900 ft (580 m) high and rises 350 ft (107 m) above the surrounding plains. To the north and east rises the remainder
Selected exposures of Pennsylvanian rocks in western Kentucky
Authors: Whaley Peter W.
Published: November 2007

Pennsylvanian rocks of western Kentucky are exposed in road cuts along Pennyrile and Kentucky Parkways north of Hopkinsville, Kentucky (Fig. 1). All stops are very accessible, but utmost caution should be exercised since these stops are on highways that carry moderate to heavy traffic. Year-round camping facilities with showers are available at John J. Audubon State Park near Henderson, Kentucky, and seasonal camping facilities with showers are available at Pennyrile Forest State Park near Dawson Springs, Kentucky (Fig. 1).
The Browns Mountain anticlinorium, West Virginia
Authors: Kulander Byron R. , Dean Stuart L. , Lessing Peter
Published: November 2007

The Browns Mountain section is located on the Marlinton and Minnehaha Springs 7½-minute quadrangles, along West Virginia 39 between Huntersville and Minnehaha Springs, Pocahontas County, West Virginia (Fig. 1). All stops along the section are adjacent to, or a short walk from, the main road and are easily accessible by bus or automobile.
Stratigraphic and structural features of Fincastle Valley and Eagle Rock Gorge, Botetourt County, Virginia
Authors: Rader Eugene K. , Gathright Thomas M.
Published: November 2007

Stratigraphic and structural features of Fincastle Valley and Eagle Rock Gorge are exposed along U.S. 220 between Fincastle and Eagle Rock, Botetourt County, 'Virginia (Fig. 1).
Batoff Creek section of Pennsylvanian-Mississippian strata, Raleigh County, West Virginia
Authors: McColloch Gayle H.
Published: November 2007

Located along West Virginia 41 between Beckley and Prince, Raleigh County, West Virginia (Fig. 1), the site is partially in the New River Gorge National River area on the north side of Batoff Creek.
Mississippian facies of the Newman Ridge area, Hancock County, Tennessee
Authors: Hasson Kenneth O.
Published: November 2007

Excellent exposures of Mississippian strata occur in road cuts on Indianand Newman Ridges, Sneedville and Howard Quarter 7½-minute quadrangles (Hancock and Claiborne counties) (Fig. 1). All outcrops are on public roads accessible by car; the Newman Ridge area can be reached via Tennessee 33 either from the south or east. Parking can be a problem at Stops 1 and 3 becausethe shoulders of the road are narrow (refer to Figs. 1 and 2 for stop locations).
Cumberland Plateau décollement zone at Dunlap, Tennessee
Authors: Wilson Robert L. , Wojtal Steven F.
Published: November 2007

The Cumberland Plateau décollement zone is exposed on Tennessee 8, 2.3 mi (3.8 km) northwest of the junction of the Tennessee 8 and U.S. 127 north of Dunlap, Tennessee (Fig. 1), Savage Point, 7½-minute quadrangle. Deformed rocks, exposed along the northeast side of the highway, in almost continuous outcrop for more than 1.3 mi (2.2 km), denotes the décollement zone. Wide shoulders along the roadway will accommodate groups of up to 50 persons.
Whiteoak Mountain synclinorium, Bradley County, Tennessee
Authors: Wilson Robert L.
Published: November 2007

Part of the Whiteoak Mountain synclinorium is exposed near the Hamilton-Bradley County line along I-75 about 21 mi (33.8 km) east of downtown Chattanooga (Fig. 1), Snow Hill, 7½-minute quadrangle. Wide shoulders along the roadway permit vehicular parking, although prior permission for stopping should be obtained from the Tennessee Highway Patrol. This stop displays superb exposures of Valley and Ridge faults and folds.
Geology of Lookout Mountain, Georgia
Authors: Cramer Howard Ross
Published: November 2007

Lookout Mountain is in Dade and Walker Counties, Georgia, in a relatively rural part of the state. However, it is near interstate access roads and lends itself well to field trips. Six stops, designed to show the major stratigraphic units of the region, are, save for one, on public land readily accessible by automobile. The Mountain cradles Cloudland Canyon State Park, which includes camping facilities. Most of the stops are on the Durham 7½-minute quadrangle; one is on the adjacent Trenton quadrangle, to the west. Figure 1 shows the locality and accessibility of Lookout Mountain.
Ringgold Gap
Authors: Rindsberg Andrew K. , Chowns Timothy M.
Published: November 2007

North end of Taylor Ridge, on south side of I-75, southeast of Chattanooga, Tennessee, 10 mi (16 km) southeast from junction of I-24 and I-75. Catoosa County, Georgia, Ringgold 7½-minute quadrangle. Accessible from I-75 or via frontage road eastward from the western of two Ringgold exits (Georgia 151, Fig. 1). The cut may be conveniently examined away from traffic on the first or second terrace.
Early Cambrian elastics in northern Cleburne and Calhoun Counties, Alabama
Authors: Bearce Denny N.
Published: November 2007

Northeast side of Cleburne County Road 70, 1.5 mi (2.4 km) west of Borden Springs and 6.25 mi (10.1 km) east of Piedmont, NW¼ Section 5, T.13S., R.11E., Cleburne County, Borden Springs 7½-minute quadrangle, Alabama (Fig. 1).
Middle and Upper Ordovician stratigraphy of the southernmost Appalachians
Authors: Neathery Thornton L. , Drahovzal James A.
Published: November 2007

Facies changes in Middle and Upper Ordovician stratigraphy can be seen in a series of exposures on I-59 and Alabama 77 in the vicinity of Gadsen, Alabama (Fig. 1).
The Jeptha Knob cryptoexplosion structure, Kentucky
Authors: Seeger C. Ronald
Published: November 2007

The Jeptha Knob Structure is on the Shelbyville and Waddy, 7½-minute quadrangles in Shelby County, Kentucky, 5 mi (about 8 km) east of Shelbyville (Figs. 1, 2). The center is at about 38°10′ N latitude and 85°07′ W longitude. It is a topographic high, extending up to small flat-topped knobs at about 1180 ft (360 m). It can be reached by automobile on routes I-64 or US 60 east from Louisville or west from Lexington. Note that Stop 3 is on a private farm, and permission is required from Mr. and Mrs. Robert Totten, Route 3, Shelbyville, KY, 40065.
Murphrees Valley anticline, a southeast-verging anticline in the Appalachian fold-thrust belt in Alabama
Authors: Thomas William A. , Neathery Thornton L.
Published: November 2007

A traverse of the Murphrees Valley anticline is provided by three stops along and near U.S. 231 in the vicinity of Oneonta, Blount County, Alabama (Fig. 1).
Extrusional environments of part of the Catoctin Formation
Authors: Lukert M. T. , Mitra Gautam
Published: November 2007

This site is located in Shenandoah National Park on the Appalachian Trail near the small parking area at mile 39.1 on the Skyline Drive (Fig. 1). It is accessibly by any vehicle including bus. Some agility is required in the “rock-scrambling” necessary to view part of the exposure. NOTE: Collecting is not allowed in Shenandoah National Park without special permission.
Cincinnati region
Authors: Davis R. A.
Published: November 2007

In the Cincinnati region an outstanding and readily accessible exposure of the classic Upper Ordovician section is the Riedlin Road/Mason Road locality, about 5 mi (8 km) south of Cincinnati. The site is a road-cut in Forest Hills, Kenton County, Kentucky (administratively a part of Taylor Mill, Kentucky). Access is provided by I-275 via exit 79 (Fig. 1). From the exit one travels north on Kentucky 16 (Taylor Mill Road) to the first cross-road (Riedlin Road/Mason Road) and turns right (east). From this point the section may be studied by progressing east and south for a distance of some 0.4 mi (0.7 km). The site is located on the Covington, Kentucky-Ohio 7.5-minute quadrangle (Luft, 1971).
The western edge of the Raleigh belt near Adam Mountain, Wake County, North Carolina
Authors: Stoddard Edward F. , Horton J. Wright , Wylie Albert S. , Blake David E.
Published: November 2007

This site consists of two stops, both located in the northeast quadrant of the Bayleaf 7½-minute Quadrangle, Wake County, North Carolina. The localities are immediately west of State Route 1005 (north of Bayleaf and south of North Carolina 98) and adjacent to the Upper and Lower Barton Creek arms of Falls Lake Reservoir on the Neuse River (Fig. 1).
Pilot Mountain, North Carolina
Authors: Butler James Robert
Published: November 2007

Pilot Mountain State 52, 24 mi (38 km) north km) south of Mount Airy, Park is located just west of U.S. of Winston-Salem and 14 mi (22 Surry County, Pinnacle 7½-minute quadrangle (Fig. 1). The Pilot Mountain State Park exit from U.S. 52 leads directly to the park entrance. The field trip narrative begins at the parking lot on the mountain top (Fig. 2, Location A). No rock collecting is allowed in the park without special written permit.