bluuebunny/crossref_metadata_2025_split huggingface dataset:
Starrs Cave Park, Burlington area, Des Moines County, southeastern Iowa
Authors: Glenister Brian F. , Kendall Alan C. , Person Jennifer A. , Shaw Alan-B. 
Published: November 2007

Abstract
Starrs Cave Park and Preserve is a facility situated on FlintCreek (Fig. 1) in the northern outskirts of Burlington, DesMoines County, Iowa (W½Sec.19, T.70N., R.2W.). It is administeredby the Des Moines County Conservation Board, Courthouse Burlington, Iowa 52601. Continuous exposures extending from the Late Devonian English River Siltstone through the Early Mississippian (Kinderhookian) carbonates of the North HillGroup and into the Medial Mississippian (Osagean) BurlingtonLimestone extend for 0.5 mi (0.8 km) along the east bank of FlintCreek. At low creek levels, the exposures are accessible directly from the Starrs Cave parking lot, on the west side of Flint Creekoff Irish Ridge Road. A steep foot trail down the cliffs to the eastprovides access from the northern extension of Irish Ridge Road during periods of high water.
House Springs, Missouri, roadcut and fault
Authors: Thompson Thomas L. 
Published: November 2007

Abstract
This section is a roadcut on Missouri 30 approximately 0.5mi (0.8 km) northeast of the junction of Missouri 30 with Jefferson County road MM, the turnoff tothe town of House Springs; SE¼SE¼NE¼Sec.33, T.43N., R.4E., Jefferson County, Missouri, House Springs 7½-section Quadrangle Map (Fig. 1). An excellent exposure of a northwest-trending fault is in the NW½NW½ Sec. 34, T.43N., R.4E.
I-55 roadcuts, Herculaneum-Barnhart, Missouri
Authors: Thompson Thomas L. 
Published: November 2007

Abstract
This is a sequence of roadcuts on I-55, extending from the NW¼ Sec.19, T.41N., R.6E., to the SE¼ Sec.19, T.42N., R.6E. (Fig. 1). These sections are accessible from the frontage road on the west side and from the Interstate highway. All exposures are i the Herculaneum 7½-minute Quadrangle.
Knob Lick Mountain section
Authors: Kisvarsanyi Eva B. , Hebrank Arthur W. 
Published: November 2007

Abstract
Knob Lick Mountain, in the eastern part of the St.Francois Mountains, is about 9.5 mi ( 15.2 km) south of Farmington, in St.Francois County, Missouri (Wachita Mountain 7½-minute Quadrangle). Rising to agentle elevation of 1,333 ft (400 m) above sea level, Knob Lick Mountain may be reached by following Knob Lick Tower Road for 1.1 mi (1.75 km) west of its junction with U.S. 67, just south of the village of Knob Lick (Fig. la), to the parking lot by the lookout tower a top Knob Lick Mountain (NE¼NE¼SE¼, Sec.8, T.34N., R.6E.). A panoramic view of the St. Francois Mountains is afforded from the bald, 100ft (30 m) south of the lookout tower. The intrusive contact of granite with rhyolite is exposed in an abandoned granite quarry, marked on Figure la (SW¼NE¼NE¼, Sec.8, T.34N., R.6E.), about 2,000 ft (600m) northwest from the lookout tower. Access to the quarry is provided by the old ridge road; walk 2,000 ft (600 m) due northwest from the lookout tower on old ridge road, then 200 ft (60 m) due east through the woods to the quarry. Visit of this site involves about a 1.5-hour hike. The site is on public land.
Elephant Rocks
Authors: Kisvarsanyi Eva B. , Hebrank Arthur W. 
Published: November 2007

Abstract
SE¼SE¼NE¼Sec.15, T.34N., R.3E., Elephant Rocks State Park, Iron County, Missouri; Graniteville 7½-minute Quadrangle. Entrance to the park isfrom Missouri RA,0.7 mi (1.2km) west of its junction with Missouri 21 (Fig. 1). From the parking lot, follow marked trail to the lookout point near the top of the hill.The site is on public land.
Baird Mountain Quarry, southwestern Missouri
Authors: Thompson Thomas L. 
Published: November 2007

Abstract
This section is in a quarry on the west side of Baird Mountain, 1.3 mi (2 km) southeast of Table Rock Dam; NW½SW½NW½Sec.26, T.22N., R.22W., Taney County, Missouri, Table Rock Dam 7¼-minute Quadrangle (Fig. 1). It has been designated the type section of the Baird Mountain Limestone Memberof the Northview Formation (Thompson and Fellows, 1970, p. 149).
The Mount Simon Formation at Eau Claire, Wisconsin
Authors: Ostrom M. E. 
Published: November 2007

Abstract
Exposure in bluff of Chippewa River and in hill called Mount Simon in City of Eau Claire (Fig. 1), in the SW½SW½Sec.8, T.27N., R.9W., Eau Claire County (Elk Mound 7÷-minute Quadrangle). Section includes all rock exposed from top of hill called Mount Simon northwest to base of river bluff.
Cambrian stratigraphy at Whitehall, Wisconsin
Authors: Ostrom M. E. 
Published: November 2007

Abstract
Road cuts north of Whitehall on Trempealeau County Highway “D” and 1.7 mi (2.7 km) north of its juncture with Wisconsin 53 in the SW¼, SW¼, Sec.12, T.22N., R.8W., Trempealeau County, on the Pleasantville 7½-minute Topographic Quadrangle, 1973) (Fig. 1).
The Platte River and Todd Valley, near Fremont, Nebraska
Authors: Wayne William J. 
Published: November 2007

Abstract
From a high point on the south side of the Platte Valley, 4.7 mi (7.5 km) west of Fremont (Fig. 1) and 1.8 mi (2.9 km) north of Cedar Bluffs (SE½SE½ Sec.22, T.17N., R.7E.; Fremont West 7¼-minute Quadrangle), one can view the present Platte River and valley as well as look across an abandoned valle segment through which at least part of the Platte River once flowed (Fig. 2). In addition, the south bluffs of the Platte, which have remained cleanly swept exposures of a large partof the Pleistocene record of eastern Nebraska since before 1900, can be seen from across the river in Hormel Park (N edge SW½Sec.34, T.17N., R.8E.) (Fig.3).
To reach the overview point, follow Nebraska 109 north from Wahoo to Cedar Bluffs, go east 0.25 mi (400 m), then north 2 mi (3.2 km) to County Road 2. Turn west 0.1mi (0.2 km) and stop at the top of the slope (Fig. 1). To reach Hormel Park in Fremont, return to Nebraska 109 and turn east 5 mi (8 km). At U.S. 77, turn northfor 1.5 mi (2.5 km), then west 0.4 mi (0.6km). Follow the gravel road to the southwest about 0.2 mi (0.3 km)to Hormel Park. Drive about 0.2 mi (0.3 km) farther, park, and walk to the edge of the Platte River. Field glasses are useful to examine the bluffs, which are across the river, about 600 ft(200 m) away.
Both the overview point
St. Lawrence and Jordan formations (Upper Cambrian) south of Arcadia, Wisconsin
Authors: Ostrom M. E. 
Published: November 2007

Abstract
Composite section from outcrops and quarries located along Wisconsin 93 (Fig. 1) and extending from 1.8 mi (2.9 km) to 3.5 mi (5.6 km) south of its intersection in Arcadia with Wisconsin 95, in the W¼, NW¼, Sec. 9, T.20N., R.9W., Trempeauleau County (Tamarack 7½-minute Quadrangle, 1973).
Cyclothems in the Carbondale Formation (Pennsylvanian: Desmoinesian Series) of La Salle County, Illinois
Authors: Trask C. Brian 
Published: November 2007

Abstract
The site is located in Sec.8, T.32N., R.2E., La Salle County, Illinois (Fig. 1), on the south bank of the Vermilion River,0.5 mi(0.8 km) west (downstream) of the town of Lowell (Fig. 2). It isin the Margery C. Carlson Nature Preserve owned by the Illinois Department of Conservation. Groups of more than 25 peopleshould check with the site superintendent at Starved Rock StatePark before entering the Preserve. For photographic purposes, thesite can be viewed from the opposite bank, which is ccessiblethrough abandoned clay pits owned by Roy Alleman, Jr. (VillageInn, Tonics, Illinois, 815-442-3535).
Ordovician-Silurian unconformity at Kankakee River State Park, Illinois
Authors: Mikulic Donald G. , Kluessendorf Joanne 
Published: November 2007

Abstract
Upper Ordovician and Silurian rocks are well exposed in aseries of natural outcrops along the Kankakee River from Wilmingtonto Kankakee, Illinois. Some of the best exposures occurin Kankakee River State Park, which extends northwest from the town of Altorf for about 6 mi (9.6 km) (Fig. 1). Thre sites are particularly interesting (Fig. 2).
1. Chippewa Campground—a river bluff on the north sideof the river just below the campground (NW¼NE¼SE¼, Sec.36, T.32N., R.10E., Bonfield 7½ minute Quadrangle, WillCounty).
2. Cowan’s Quarry—abandoned stone pits and river bluffson the north side of the river between the river and State Highwa102 (SE½SW½NW½, Sec.26, T.32N., R.10E, Bon field 7½-minute Quadrangle, Will County).
3. Rock Creek—a canyon of a tributary north of the KankakeeRiver, north and south of the bridge on State Highway 102(S¼SE¼SW¼, Sec.32, T.32N., R.11E., Bourbonnais 7½-minuteQuadrangle, Kankakee County).
All localities except Cowan’s Quarry are accessible by passenger car and are a short walk from a highway or parking lot.Cowan’s Quarry is reached by an unmarked and unmaintaineddirt road leading south to the river from Illinois 102 (Fig. 2). This road is generally in poor condition, but is the only place to park as there is no shoulder on the highway. From the dirt road, walkwest about 300 ft (100 m) along the top of the river bluff to theold stone pits.
Valmeyer Anticline of Monroe County, Illinois
Authors: Norby Rodney D. 
Published: November 2007

Abstract
Strata of the Valmeyer Anticline are exposed in road anstream cuts along Illinois 156 (Fig. 1), which passes throughDennis Hollow from the east edge of Valmeyer to 1.5 mi (2.4km) east of Valmeyer, Monroe County (Sec.2, SE¼SE¼Sc.3, and N½Sec.10, T.3S., R.11W.; Valmeyer 7.5-minute Quadrangle);they are also exposed in the bluff face at Columbia QuarryPlant No. 3, which is 0.9 mi (1.5 km) north of Valmeyer(SE¼NW¼Sec.3, T.3S., R.11W.). The outcrops along Illinois 156are easily accessible with no more than a 300 ft (100 m) walkfrom the highway. Automobile parking is limited to a few widegrassy pullouts adjacent to the south side of the highway andalong driveways of property owners. The area north of Illinois156 has several owners; therefore permission to enter should beobtained from residents nearest a particular outcrop.
Horseshoe Quarry, Shawneetown Fault Zone, Illinois
Authors: Nelson W.John 
Published: November 2007

Abstract
The Horseshoe quarry is located in the SW¼, NW¼, NE¼, Sec.36, T.9S., R.7E., Saline County; Rudement and Equality 7½-minute QuadrangleIllinois (Figs. 1, 2). From Equality, travel south 2.0 mi (3.2 km) via county road to the foot of Wildcat Hills, then west 2.5 mi (4 km) on gravel road to a point 0.2 mi (0.3 km) past the turnoff to Glen O. JonesLake. The longabandoned quarry is in low, wooded hills immediately north of the road, on land administeredby the U.S. Forest Service.
The Cache Valley of southern Illinois
Authors: Masters John M. , Reinertsen Davis L. 
Published: November 2007

Abstract
The Cache Valley in extreme southern Illinois is amajor physiographic feature that extends across all or parts of Pope, Massac, Johnson, Union, Pulaski, and Alexander counties, from the Ohio River on the east to the Mississippi River on the west, and cuts across all or parts of the following Third Principal Meridan townships (Fig. 1): T.13S., R.3, 5, and 63; T.14S., R.1, 2, 3, 4, 5, and 6E, R.1 and 2W; T.15S., R.1, 2, 3, and 4E., R.1, 2, and 3W;T.16S., R.1, 2, 3, and 4W; and T.17S., R.1 and 2W.
Devonian shelf-basin, Michigan Basin, Alpena, Michigan
Authors: Gutschick Raymond C. 
Published: November 2007

Abstract
This chapter cites two localities, Paxton Quarry and Partridge Point (Fig. 1), and combines field observations fromboth to illustrate important stratigraphic relations and principles.Focus is on litho- and biostratigraphyof Middle and Late Devonian rocks as they relate to the Michigan Basin (Fig. 2).
Black organic-rich shales deserve our attention due to their energy potential asource rocks and fracture reservoirs for petroleum and natural gas. The Paxton Quarry offers the opportunity to examine an exceptional exposure of black shale (large area in Fig. 3; thick section in Fig. 4) as part of the formational sheet that continues into the Michigan Basin subsurface. These special rocks offer achallenge to observe and test their physical, chemical, and organic composition and structureto decipher origin, paleoenvironments, diagenesis, history, and economic value. A spectacular display of numerous, largecalcareous concretions, in situ and free of shale matrix, is present in the quarry. How werethey formed?
Partridge Point has an exposed limestone sequence that underlies Antrim black shales beneath Squaw Bay. Applying Walther’s Law, one can go up section and down dip from fossiliferous shallow-water oxygenated Middle Devonian carbonate platform rocks at the shelf marginof the Michigan Basin into Upper Devonian transitional deeper water oxygen-deficient pelagic limestones followed by deep-wateranaerobic black shales of a euxinic basin.
Mississippian Marshall Formation of the Pointe Aux Barques region, eastern Michigan
Authors: Milstein Randall L. 
Published: November 2007

Abstract
Pointe aux Barques Region T.18N., R.1lE. and T.19N., R.13E., Huron County, Michigan; Rush Lake, Port Austin West, Port Austin East, and Kinde West, Michigan, 7½-minute quadrangles.The Pointe aux Barques region ofHuron County extends east from Little Oak Point 18 mi(29 km) along the Lake Huron shoreline to Grindstone City (Fig.1).The Pointe aux Barques area is reachedby following Michigan 53 north from Bad Axe to Port Austin. This picturesque shoreline region is also accessible by boat.
The Indiana Dunes area, northwestern Indiana
Authors: Hill John R. 
Published: November 2007

Abstract
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

Abstract
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

Abstract
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

Abstract
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

Abstract
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

Abstract
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.