bluuebunny/crossref_metadata_2025_split huggingface dataset:
Quaternary basalt fields of west-central New Mexico
Authors: Elston Wolfgang E. , Wohletz Kenneth H. 
Published: November 2007

Abstract
The U.S. Geological Survey was only five years old when its director, John Wesley Powell, approved Captain Clarence Dutton’s plan for one field season on Mount Taylor and the Zuni Plateau (Fig. 1). Dutton’s description of west-central New Mexico, published in 1885 as part of the U.S. Geological Survey’s 6th Annual Report, has become a geologic classic, not only for its lucid literary style but also because it laid the foundation of basic geologic concepts. In his account of erosion and uplift, the reader can discern the germ of ideas that would lead Dutton within four years, to the principle of isostasy. In a discussion of mountain building, he contrasted compressional fold belts, such as the Alps and Appalachians, with mountains of western interior North America, in which vertical uplift and rifting had been the principal forces. Finally, he pondered the significance of the great volcanic fields that nearly encircle the Colorado Plateau.
In the Mount Taylor-Zuni area, Dutton recorded a history of volcanism from late Tertiary to late prehistoric time. Basalt predominates; the youngest lavas issued from cones that are still well preserved, and the lava flowed down modern valleys. Older lavas cap mesas (in general, the higher the mesa, the older the cap; see Fig. 2), 2), and many of their vents have been reduced to volcanic necks. There are dozens of small basalt volcanoes in various stages of preservation as well as one large central volcano (Mt. Taylor, elevation 11,389 ft; 3472 m)
Geology of the Butte mining district, Montana
Authors: Zeihen Lester G. , Berg Richard B. , McClernan Henry G. 
Published: November 2007

Abstract
The Butte mining district is in Silver Bow County in southwestern Montana at the intersection of 1-15 and 1-90. The district proper lies north and west of these highways, and most of it is within the business and residential areas of Butte. Because city streets provide access to all of the stops, they are easily accessible by automobile or on foot as shown in Figure 1. The sites described lie on private land and direct access is not practical to most of them; however, because of their large size they can be easily viewed from the public right of way. A pair of binoculars is useful in viewing some of these features. Unfortunately, the best exposures of veins are in the underground workings no longer accessible or in open pits to which access is prohibited.
The Jefferson River Canyon area, southwestern Montana
Authors: Schmidt Christopher , Aram Richard , Hawley David 
Published: November 2007

Abstract
The Jefferson River Canyon area is on an important structural boundary between the Cordilleran thrust belt and the Rocky Mountain foreland (Fig. 1). The features described here reflect the tectonic history of that boundary from late Precambrian through late Cenozoic time. The area is in Jefferson and Madison counties. Most of the features described may be observed along U.S. 10 through the canyon and along the access road to the Lewis and Clark Caverns State Park (Fig. 2). Stops of particular interest discussed in the text are numbered and indexed in Figure 2 with mileages indicated from LaHood Park (bar, restaurant, and sometime gas station and motel) and/or from the intersection of U.S. 10 and the state park access road. The area is located in the center of the Jefferson Island 15-minute Quadrangle.
Many of the features that can be seen across the Jefferson River from U.S. 10 (south side of river) are currently accessible via the abandoned track bed of the Chicago, Milwaukee, St. Paul, and Pacific Railroad. The track bed is easily traversed by most vehicles and may be accessed on the west from County Road 359 at Jefferson Island and on the east from Montana 287 at Sappington. The access route at Jefferson Island is privately owned and the owner (Vernon Shaw of Cardwell) should be contacted for permission.
Upper Ordovician Maquoketa Formation in the Graf Area, eastern Iowa
Authors: Witzke Brian J. , Glenister Brian F. 
Published: November 2007

Abstract
James Hall (1858) was the first to recognize that a shaledominatedinterval, the Hudson River Group, separates the Galena Limestone (Middle-Upper Ordovician) from the overlying Niagara Limestone (Silurian) in eastern Iowa. Hall’s primary exposure of these rocks was located in the Little Maquoketa River Valley near present-day Graf, Iowa. There he observed“orthoceratite beds, ” graptolitic shales, and an abundance of “extremelysmall” fossils. Charles White (1870) named this sequenceof bluish and brownish shales the Maquoketa Shales after “typicallocalities on the Little Maquoketa River about twelve mileswestward from Dubuque” (i.e., near Graf). Joseph James (1890) described a railroad cut exposed in 1886 near the Graf station, which he termed the “typical locality of the shales in Iowa.” Thissame section is accessible today, but has been expanded to thenorthwest by subsequent road construction. Additional descriptions of the Graf section are givn by Calvin and Bain (1900), Thomas (1914), and Tasch (1955).
The Graf section (S½NW¼SW¼Sec.29, T.89N., R.lE., DubuqueCounty) is recognized as the type locality of the Upper Ordovician Maquoketa Formation, although the bulk of the Maquoketa Shale sequence in the area is represented by covered slopes. Access to this section is most convenient from the southon gravel roads that begin 0.5 mi (0, 8 km) west of the intersection of Old U.S. 20 and County Road Y21 (Figs. 1, 2). The Maquoketa Formation throughout the outcrop belt of northeast Iowa is expressed geomorphically as covered slopes to rollingsurfaces
Roadcuts in the St.Francois Mountains, Missouri
Authors: Kisvarsanyi Eva B. , Hebrank Arthur W. 
Published: November 2007

Abstract
This composite site features roadcuts along U.S.67 and Missouri 72 in the eastern St.Francois Mountains, in Madison County, Missouri (Fig. 1).
STOP 1 (NW¼SW¼NE¼Sec.35, T.34N., R.6E.), along U.S.67 is 14.8 mi (23.7 km) south of the junction, west of Farmington, of U.S.67 and Missouri W. It is located on the Fredericktown 7½-minute Quadrangle. Roadcuts at this stop display a basalt-dike swarm in the Precambrian Slabtown Granite.
STOP 2 (NE¼SE¼NW¼Sec.11, T.33N., R.6E.) is along Missouri 72; from STOP 1, proceed 2.7 mi (4.3 km) south on U.S.67, then 1.8 mi (2.9 km) west on Missouri 72 (Fig. 1). Roadcuts at this locality expose the nonconformable contact between Precambrian and Paleozoic rocks in a spectacular manner.
STOP 3 (NE¼NE¼NE¼Sec.9, T.33N., R.6E.) is 1.7 mi (2.7km) west of STOP 2, along Missouri 72 (Fig. 1). It is located on the Rhodes Mountain 7½-minute Quadrangle. This site displays horizontally bedded, channel-fill sediments within basal boulder conglomerate mantling the Precambrian surface.
Johnson Shut-ins
Authors: Hebrank Arthur W. , Kisvarsanyi Eva B. 
Published: November 2007

Abstract
Johnson Shut-ins State Park, W½Sec.16 and NW¼Sec.21, T.33N., R.2E., Reynolds County, Missouri; Johnson Shut-ins7¼-minute Quadrangle. Entrance to the park is from Missouri N(Fig. 1), 13.2 mi (21 km) southwest of its junction with Missouri 21, north of Ironton, Missouri, and 6.2 mi (10 km) northeast of its junction with Missouri 21–49–72, west of Lesterville, Missouri.From the parking lot, walk east on well-marked (paved) trailabout 1800 ft (540 m) to the shut-ins overlook(Fig. 2).The site is on public land.Note State parkrules prohibit defacing or collecting rocks.
Baraboo Quartzite at Skillett Creek, Wisconsin
Authors: Brown B. A. 
Published: November 2007

Abstract
The exposure is on the east side of U.S. 12, 0.3 mi (0.5 km) south of the junction with Wisconsin 159, SW¼, NW¼, Sec. 15, T.–11N., R.6E., North Freedom 7½-minute Quadrangle (Fig. 1). Caution: Traffic on U.S.12 is heavy, and there is a blind curve just north of the outcrop.
Middle Silurian paleoecology; The Raber Fossil Beds, Chippewa County, Michigan
Authors: Milstein Randall L. 
Published: November 2007

Abstract
The Raber Fossil Beds are in Sec.32, 33, 34, T.43N., R.3 E., and to the general public for their unusual scenic appeal. Collectand Sec.3–5, 8–11, T.42N., R.3E., Chippewa County, Michigan; ing of fossil specimens on tate-owned land is discouraged. Pres-Goetzville, Michigan, 7½-minute Quadrangle. The RaberFossil ently, theRaber area is under review as a potential protected Beds are located roughly 1 mi (2 km) south and southeast of the Natural Area. Within such a Natural Area the collecting of specvillage of Raber, on the St. Marys River (Fig.1).
The area is accessible from two points. A trail from near the Privately-owned land surrounding the state property offers Bernard Farm leads in a southeasterly direction 0.5 mi (0.8 km) many tine collecting areas. Permission must be gained from land to the base of a low rock escarpment and follows this escarpment owners prior to entryon their property. for an additional 0.5 mi (0.8 km) where the trail branches and Visitors to the Raber site should prepare themselves adecontinues to the top of the ridge. A second point of access is by quately for hiking through rough, often uneven wooded terrain. means of a road extending directly east of Goetzville which is From early spring to late autumn, biting insects can be passable for approximately 0.5 (0.8 km) into the area. Other bush bothersome. trails into the area are not readily passable by automobiles.
The majority of land in which the Raber Fossil Beds exist is Raber area contains the ruins
Mackinac Island State Park, Michigan
Authors: Milstein Randall L. 
Published: November 2007

Abstract
Mackinac Island State Park, T.40N., R.3W., Mackinac County, Michigan; Cheboygan, Michigan, U.S.G.S. 30 × 60 minute series. Mackinac Island is located 3 mi (5 km) east of St. Ignace, Michigan, in the Straits of Mackinac (Fig. 1). Access to the Island from St. Ignace is provided by Arnold Transit or Star Lines from mid-April to late-December. From Mackinaw City, service is provided by Arnold Transit or Shepler’s Mackinaw Island Ferry from mid-May to mid-October. Service is at least hourly during the summer months. Air charter service is provided by Great Lakes Charters, St. Ignace, or Michigan Airways, Pellston. From December to mid-April, transportation is by Air Charter Service only from the Mackinac County Airport, St. Ignace. No motorized vehicles are permitted on Mackinac Island. On the Island, transportation is available in the form of rental bicycles, horses and horse drawn carriages.
Fort Wayne, Indiana
Authors: Sunderman Jack A. 
Published: November 2007

Abstract
The geology displayed in and around the city of Fort Wayne, Indiana, is interesting and critically important for at least two reasons: (1) a large quarry near the city exposes an unusual variety of Paleozoic strata, some facies of which are not exposed at any other place; and (2) the city is situated at the junction of several Pleistocene glacial features of regional significance (Fig.1).
The largest and most spectacular quarry in northeastern Indiana is the Ardmore Avenue Quarry of May Stone and Sand, Inc., located along Ardmore Avenue in the NE¼Sec.29, T30N., R.12E. on the southwest edge of Fort Wayne (Figs.1), 2). This quarry is one of the two largest and deepest crushed-stone quarries in Indiana, measuring more than 2,000 ft (610 m) across in a northeast-southwest direction and about 271 ft (82 m) deep during the fall of 1983 (Fig.3). The quarry is readily accessible for public viewing from a stand provided by the company on the north side of the quarry. Thisstand allows such an instructive and spectacular view of the quarry that it has become the focal point for most field trips to the area. Those desiring to enter the quarry should direct their inquiries to the Ardmore Avenue office of May Stone and Sand, Inc.
The Ardmore Avenue Quarry is also the focal point for the study of Pleistocene features in this area because of the excellent exposures of a complex Pleistocene section at the top of
The Falls of the Ohio River, Indiana and Kentucky
Authors: Rexroad Carl B. , Powell Richard L. 
Published: November 2007

Abstract
The Falls of the Ohio River is internationally renowned for the profusion of corals and other fossils found in the Devonian beds at this site. Indeed, the earliest paper on its corals was published in Belgium by Rafinesque and Clifford in 1820. Subsequently, about 75 papers have described some 600 fossil species fromthe falls, Other studies have addressed the geomorphology of the area, including in particular the origin and history of the Ohio River and of the falls. The Falls of the Ohio is also important in understanding the Devonian history of southern Indiana and adjacent Kentucky.
In reality a series of rapids, the Falls ofthe Ohio encompassed a stretch of the Ohio River about 2 mi (3.2 km) long between Louisville, Kentucky, onthe south bank of the river, and New Albany, Clarksville, and Jeffersonville, Indiana, on the northern bank (Fig. 1). “In these rapids, the river has a descentof twenty-two and a half feet, … but in no case, has it a perpendicular fall of more than three. At high water, an acceleration of current, not usual to other parts of the river, is all that is perceived; but at low water, it cannot be passed by loaded boats, without great risk and danger” (Lapham, 1828). Therefore, the Falls Cities owe their initial growth and development to the fact that during times of low water, boats following this major artery of westward expansion either had to off-load and portageor had to wait for high water.
The Cuyahoga Valley National Recreation Area, Ohio
Authors: Hannibal Joseph T. , Feldmann Rodney M. 
Published: November 2007

Abstract
The Cuyahoga Valley National Recreation Area is located along the Cuyahoga River Valley between Cleveland and Akron, Ohio (Fig. 1). Major interstate highways, including I–77, 1–80, and I–271, as well as several Ohio state routes, pass near, or The Cuyahoga Valley National Recreation Area contains through, the National Recreation Area. The sites discussed are excellentexposures of several of northeastern Ohio’s classic and located within three parks that are part of the National Recrea-well-studied Paleozoic rock units. In Brecksville Metropark rockstion Area. Although one candrive to each of the three sites, final The Cuyahoga Valley National Recreation Area is located access requires some hiking, primarily along park trails.
Flint Ridge, Ohio
Authors: Carlson Ernest H. 
Published: November 2007

Abstarct
Flint Ridge is located in southeastern Licking and western Muskingum counties in east-central Ohio (Fig. 1). Geologicalninterest centers on Flint Ridge State Memorial and a roadcut exposure nearby (Fig. 1, 2). This area can be reached easily from Brownsville by taking 1-70 to the Brownsville exit, if traveling east, or to the Gratiot exit and continuing west on U.S. 40 for 1.9 mi (3 km), if traveling west (Figs. 1), 2). The memorial is situated 3 mi (5 km) north of Brownsville where Licking County Road 668 intersects Flint Ridge Road (Licking County Road 312). Access to the backbone of the ridge is provided by Flint Ridge Road, which runs east and west from the memorial.
The memorial includes a museum (built over a prehistoric Indian quarry), a trail that winds through old flint workings, picnic facilities, and a parking area, It is open from April through October, but closed Mondays. The roadcut exposure is reached by walking 0.2 mi (0.3 km) north of the memorial along Licking County Road 668. No parking is available here, and due to the sharp curve and traffic along the road, caution must be observed at all times. Exposures of flint can also be observed on two tracts of private land if appropriate arrangements are made. The owners are Clayton Mason, in Licking County, 0.9 mi (1.5 km) east of the memorial on Flint Ridge Road, and John Nethers, in western Muskingun County on
Igneous geology of the Wichita Mountains, southwestern Oklahoma
Authors: Gilbert M. C. , Powell B. N. 
Published: November 2007

Abstract
The Wichita Mountains extend for about 65 mi (105 km) northwest from Lawton, Oklahoma (Fig. 1). Four sites are described here: 27—Quartz Mountain State Park in the western part of the Wichita Mountains, near Oklahoma 44A; 28—The Tom Steed Reservoir area, along U.S. 183 in the central Wichita Mountains; 29—French Lake, south of Oklahoma 49; and 30—the Mt. Scott area, north of Oklahoma 49 in the eastern Wichita Mountains. Specific directions to each site are given with the site descriptions.
Great Salt Plains and hourglass selenite crystals, Salt Fork of the Arkansas River, northwest Oklahoma
Authors: Johnson Kenneth S. 
Published: November 2007

Abstract
The Great Salt Plains comprise about 25 mi2 (64 km2) of flat, barren land, naturally encrusted with salt (halite), along the Salt Fork of the Arkansas River (Fig. 1). The salt plains, which also embrace the area where unique hourglass selenite crystals are currently growing, are almost entirely enclosed within the Great Salt Plains National Wildlife Refuge. Located in central Alfalfa County, Oklahoma, the land is about 4 mi (6.4 km) east of Cherokee and just northwest of Jet. Free access by car or bus is permitted at all times during the year to the salt flats in the vicinity of the observation tower on the west (site 1, Fig. 1) and to the dam and state park area in the east (including picnic and camping facilities and cabins). Also, free access by car or bus to the selenite crystal area (site 2, Fig. 1) is permitted through only one gate, which is unlocked from 8 A.M. until 5 P.M. only on Saturdays, Sundays, and holidays from April 1 to October 15 each year. The crystal area is about 1 mi (1.6 km) northeast of this gate and can be reached safely by driving along the specified road across the salt flats. Access to other parts of the Great Salt Plains is restricted by fences; quicksand, at scattered locations on the salt flats, makes trespass in nonauthorized areas hazardous. The area is covered by four 7½-minute quadrangle maps: Cherokee S, Cherokee N, Jet, and Manchester SW. For information concerning the
Shelf to slope facies of the Wapanucka Formation (lower-Middle Pennsylvanian), frontal Ouachita Mountains, Oklahoma
Authors: Grayson Robert C. , Sutherland Patrick K. 
Published: November 2007

Abstract
Two transects examine shelf-to-slope facies relations of the Wapanucka Formation in southeastern Oklahoma near the towns of Pittsburg and Hartshorne (Fig. 1). Detailed directions to several localities along each transect are given in the text.
Depositional and deformational characteristics of the Atoka Formation, Arkoma Basin, and Ouachita frontal thrust belt, Oklahoma
Authors: Houseknecht David W. , Underwood Michael B. 
Published: November 2007

Abstract
Sedimentary facies and structure of the Atoka Formation of the Arkoma basin and Ouachita frontal thrust belt are illustrated by a north-south transect in LeFlore County, Oklahoma.
Locality 1 (94°29—32’W.; 35°12—30"N.; Hackett Quadrangle) is a roadcut on Oklahoma 112, 1.5 mi (2.4 km) south of the village of Pocola (Fig. 1). The Atoka Formation crops out along the Backbone anticline, which is the expression of a thrust fault that ramps to the surface just north of this exposure. The exposed strata are correlative with the ‘Alma’ sandstone of subsurface terminology; in this part of the basin, the Alma is located about 2,650 ft (800 m) below the top and 4,650 ft (1,400 m) above the base of the Atoka Formation. The strata dip 45° to the south.
Locality 2 (94°38—06’W.; 34°49—36’N.; Hodgen Quadrangle) is a roadcut on U.S. 270/59, 1.1 mi (1.8 km) south of the village of Hodgen (Fig. 1). This north-dipping Atoka section is exposed just south of the Choctaw thrust fault (south of the Choctaw fault, the Atoka has been renamed the Lynn Mountain Formation in certain recent publications).
Locality 3 (94°37—37’W.; 34°44—46—N.; Big Cedar Quadrangle) is a roadcut on U.S. 270/59 just south of the village of Stapp. These strata have traditionally been placed within the Johns Valley Shale (Seely, 1963; Hart, 1963), but recent mapping indicates that the turbidites and debris-flow deposits are simply one of several facies associations within the Lynn Mountain Formation (Poole, 1985; McDonald, 1986). The section is slightly overturned to the
Basal sandstone of the Oil Creek Formation in the quarry of the Pennsylvania Glass Sand Corporation, Johnston County, Oklahoma
Authors: McPherson J. G. , Denisen R. E. , Kirkland D. W. , Summers D. M. 
Published: November 2007

Abstract
The basal sandstone of the Oil Creek Formation is well exposed in a quarry located 5 mi (8 km) north northwest of the small town of Mill Creek in Johnston County, Oklahoma (Sec.14, T.1S., R4E.) (Figs. 1 and 2). The quarry is owned by the Pennsylvania Glass Sand Corporation and is about 0.5 mi (0.8 km) west of Oklahoma 7, which passes through Mill Creek and connects with I-35 about 20 mi (32 km) to the west.
Middle Ordovician strata of the Arbuckle and Ouachita Mountains, Oklahoma; Contrasting Lithofacies and biofacies deposited in southern Oklahoma Aulacogen and Ouachita Geosyncline
Authors: Finney Stanley C. 
Published: November 2007

Abstract
Middle Ordovician strata of the Arbuckle and Ouachita Mountains record markedly different depositional settings (Figs. 1, 2). Three localities in the Arbuckles and one in the Ouachitas demonstrate both the vertical sequences of Lithofacies within each area and the contrasts in Lithofacies and biofacies between the two areas.
Localities 1 through 3 (Fig. 1) are in the Arbuckle Mountain region. Locality 1 (Fig. 3) is in the northeastern part of the Arbuckles. It consists of a roadcut exposure along the west side of Oklahoma 99, about 3.5 mi (5.6 km) south of Fittstown, SW¼Sec.12, T.1N., R.6E., Pontotoc County. It is readily accessible and requires no permission to visit. Locality 2 (Fig. 3) is a long roadcut along the west side of the southbound lanes of I-35 on the south flank of the Arbuckle Mountains. It is in the SW¼Sec.25, T.2S., R1E., Carter County, is readily accessible, and requires no permission to visit. Locality 3 (Fig. 3) is at the north end of Criner Hills. It is a small quarry situated in the SW¼SE¼- Sec.9, T.5S., R.1E., Carter County, readily accessible from I-35 and U.S. 70 by well-maintained gravel roads. The quarry is on private land. Permission for access can be obtained from the landowner, Ronald Burns of Ardmore, Oklahoma (405- 657-8262).
Locality 4 (Figs. 1,3) is at the western edge of the Ouachita Mountains. It is the Stringtown Quarry at the north end of Black Knob Ridge, directly north of the town of Stringtown, and situated in the center of
I-35 Roadcuts; Geology of Paleozoic strata in the Arbuckle Mountains of southern Oklahoma
Authors: Fay Robert O. 
Published: November 2007

Abstract
The field-trip site consists of excellent exposures of Paleozoic strata in roadcuts along I-35 through the Arbuckle Mountains of south-central Oklahoma (Figs. 1 and 2). The exposures extend from 11 to 18 mi (18 to 29 km) north of the city of Ardmore, and are in parts of Murray and Carter Counties. Access to the roadcuts is open at all times, but extreme caution must be exercised because the exposures are along the right-of-way of a major 4-lane divided highway. Parking should be on the far right side of the shoulder, and one should not walk upon or cross the highway. If a large group is to examine the exposures, it would be best to park vehicles in the scenic turnouts and hike along the highway shoulders to examine the roadcuts.
Lithostratigraphy and depositional environments of the Springer and lower Golf Course Formations, Ardmore Basin, Oklahoma
Authors: Meek Frederick B. , Elmore R. Douglas , Sutherland Patrick K. 
Published: November 2007

Abstract
The two lower members of the Springer Formation are well exposed in the vicinity of City Lake, located northwest of Ardmore, Oklahoma. The upper member of the Springer Formation and the lower member of the Golf Course Formation are well exposed along Phillips Creek, northwest of Springer, Oklahoma (Fig. 1). Detailed directions to these localities are given in the text.