The geology of the Pine Log Creek area [1986]

THE GEOLOGY OF THE PINE LOG CREEK AREA
by
Leonard E. Foote
OPEN-FILE REPORT 86-2
NOT TO BE REMOVED FROM SUIWEY
Department of Natural Resources Environmental Protection Division
Georgia Geologic Survey
1986

THE GEOLOGY OF THE PINE LOG CREEK AREA
by Leonard E. Foote Open-File Report 86-2
Department of Natural Resources Environmental Protection Division
Georgia Geologic Survey
1986

TABLE OF CONTENTS
ABSTRACT The Geology of the Pine Log Creek Area
I. Introduction II. Acknowledgements III. Previous Geological Investigations IV. Geography V. Land Use and Vegetation VI. Regional Stratigraphy and Structure VII. Local Stratigraphy and Rock Types VIII. Depositional Environment IX. Structure X. Structure of Individual Formations XI. Water Resources XII. Mineral Resources
Literature Cited

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1 1 1 2
3 3 4 9
11 14 18 19
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ILLUSTRATIONS
Figure 1: Sample locations and place names 1n Pine Log Creek map area
Plate 1A: Geologic map of the Pine Log Creek area : Formations and Cross Sections
Plate lB: Geologic map of the Pine Log Creek area: Field data

TABLES

Table 1: Table 2: Table 3: Table 4: Table 5: Table 6:

Percentage of major oxides in spec1mens of carbonate rocks
Chemical analyses of shale samples
Percent potassium oxide in Rome Formation and Conasauga Group
Percent magnesium oxide in Rome Formation and Conasauga Group
Results of Duncan Multiple Range Test
Analyses of other elements in carbonates

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THE GEOLOGY OF THE PINE LOG CREEK AREA, BARTOW COUNTY, GEORGIA .
ABSTRACT
The structure of the Cambrian Shady Dolomite, Rome Formation, Rogersville Shale and Rutledge Limestone west of the Great Smoky fault in the northern portion of the Cartersville Mining District, Georgia, is believed to be a thrust stack of Early Paleozoic sediments underlain by a decollement fault above the basement rock contact.
The depositional environment is hypothesized to be similar to that of these formations 1n the Ridge and Valley province in Tennessee.
The relation of the Ocoee Supergroup Wilhite Formation to the Cambrian sediments is discussed, including the probability of a window ~f Rome Formation (of Kesler, 1950) dolostone existing in the overthrusting Wilhite Formation. The structure and relations of Shady dolostones, poorly understood, is treated in some detail. The abundant ground-water resources of the area are described and quantified and the mineral resources are summarized. No barite was found, although it is mined commercially in the southern portions of the Cartersville Mining District.

THE GEOLOGY OF THE PINE LOG CREEK AREA
I. INTRODUCTION
The Pine Log Creek area, as referred to here, includes the northern part of the Cartersville Mining District, Bartow County, Georgia, which is part of the eastern edge of the Ridge and Valley physiographic province. This area contains fewer known mineral deposits of economic significance than the remainder of the Cartersville Mining District; however, it previously has not been studied in detail. This study was undertaken to locate potential mineral resources and determine the major rock types and structural relations of the four Paleozoic lithologies in the area: the Chilhowee Group (Weisner Formation), Shady Dolomite, Rome Formation and the Conasauga Group.
The Pine Log Creek study area (Plate 1) comprises approximately 14 square miles (36 square kilometers) and is roughly triangular in plan with the apex to the east. It is bounded by the Great Smoky fault on the east and northeast and by U.S. Highway 411, which forms the western boundary for 5.6 miles (14.3 km), 1.8 miles (4.6 km) south of the Bartow-Gordon County line. Most of the study area is included in the northern half of the White East 7.5 minute quadrangle.
II. ACKNOWLEDGEMENTS
Special acknowledgement is made to State Geologist William H. McLemore of the Georgia Department of Natural Resources, to Mr. Thomas Crawford of West Georgia College and Mr. Charles Cressler of the U.S. Geological Survey, each of whom spent several days in the field and aided in many ways. I am indebted to Mr. Earl Shapiro of the Georgia Department of Natural Resources for editing the manuscript. Mr. Russell E. Foote of Engelhard Minerals Corporation and Mr. William Zelinski of Amoco Minerals Corporation gave interpretive assistance. I am indebted to Anita G. Harris and Katherine S. Schindlar of the U.S. Geological Survey for processing rock samples for conodonts and other fossils.
Landowners in the area freely allowed access to property and provided information on wells and springs. Special thanks are due Mr. Wesley Smith, former clerk of the Bartow County Court, for historical information and other aid,
III. PREVIOUS GEOLOGICAL INVESTIGATIONS
The Pine Log Creek area has been included in geological reconnaissances of larger areal scope for nearly a century. Beginning with Hayes (1891, 1901), the area was subsequently studied by Spencer (1893), Shearer (1918), Butts and Gildersleeve (1948), Kesler (1950), Croft (1963), Bentley, et al (1966), Cressler, et al (1979), and Davis (1984). The area was examined for sulfide minerals by Hurst and Crawford (1970); McLemore and Hurst evaluated the carbonates in the Coosa Valley area.
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Studies of adjacent areas germane to the present investigation are those of: Smith (1959) who examined the Great Smoky fault in the vicinity of Fairmount; Stuart (1953) investigated Conasauga shales and carbonates in the same vicinity; Smith (1958) reported on Conasauga rocks in the Ranger area; Cressler (1974) studied the geology and ground-water resources of adjacent Gordon County; Chowns and others (1977) examined the Cambrian and Ordovician stratigraphy in Bartow County; and Spalvins (1963) studied the Conasauga Group in the Adairsville area. Harris (1973) and Harris and Milici (1977) have described Cambrian through Lower Ordovician sedimentation of the Ridge and Valley physiographic province.
IV. GEOGRAPHY
The study area is underlain by sedimentary rocks of the Ridge and Valley physiographic province. (Place names and rock sample collection locations are shown on Figure 1.) To the east of the Great Smoky fault are the higher elevations of the overthrust crystalline rocks: Pine Log Mountain at 2331 feet (711 meters), Bear Mountain at 2303 feet (702 meters) and Johnson Mountain at 1296 feet (395 meters). To the west of the Great Smoky fault, the study area terminates at the western edge of a long, broken valley which contains U.S. Highway 411 and the railroads. Within the study area a maximum elevation of 1305 feet (398 meters) occurs at the top of the Chilhowee Group (Weisner Formation) approximately 0.5 mile (0.8 km) west of the Great Smoky fault. The lowest elevation in the area occurs where Pine Log Creek is crossed by U.S. Highway 411 at Bolivar; the elevation here is 784 feet (239 meters) above mean sea level.
Predominant features of the topography of the study area are the relatively flat valleys of Pine Log and Su~ar Hill Creeks. The terrain is northwest-trending creek valleys and rolling to slightly precipitous dissected hills which trend north-northeast.
Surface water from the average annual rainfall of approximately 50 inches (127 em) (Kesler, 1950) drains into Pine Log and Sugar Hill Creeks, which flow northwestward to eventually join the Oostanaula River in western Gordon County. At U.S. Highway 411, Pine Log Creek drains about 24 square miles (62 square km) and has an estimated flow of about 21 million gallons (79.5 million liters) per day (Cressler, et al, 1976). About one-third of its volume is derived east of the Great Smoky fault. Much of the flow from both Pine Log and Sugar Hill Creeks consists of ground water discharging from numerous springs in the study area. August water temperatures taken at several locations varied from 59 to 68 degrees F (15 to 20 degrees C). A Soil Conservation Service floodwater detention reservoir was constructed in 1975 on the Sugar Hill Creek headwaters and substantial beaver populations have created additional impoundments on both creeks.
Paved Georgia Highway 140 bisects the area and no portion of the study area is more than one-half mile from an all-weather gravel secondary road. The area is sparsely inhabited; secondary roads are used primarily to transport agricultural and forest products. Many abandoned roads, now regenerated with timber or converted to pasture, testify to denser human habitation in the past.
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V. LAND USE AND VEGETATION
Pre-colonial vegetation of the Pine Log Creek region probably consisted of Loblolly, Shortleaf, Virginia Pine and upland hardwoods. This climax vegetation included many shrub and herb species diversified by differences in soil, topography and water supply. Some plants grow only on carbonate rocks or on soils derived from them, while others occur exclusively on more acid sites. For example, two such diagnostic plant species in the Pine Log Creek area are Trillium decumbens and Gentina saponaria (Pringle, 1967).
The Pine Log Creek basin was modified by horticulture initially by Creeks, then by the Cherokees (Golf, 1963). More modern agriculture began with the great land lotteries of the 1830's. Subsistence farming slowly gave way to the mechanized production practiced today.
Although nearly half the study area is now being grazed or farmed (principally for soybeans and small grains), many more acres were tilled in the past. Most of the present pine forest has been terraced, probably to grow cotton during the past century. Substantial acreage of pine forest has been clear-cut during the past two years. The history of land ownership, beginning with the 160-acre lottery in 1832, has been one of continuous consolidation; relatively few landholders control the acreage today.
Agricultural and forest management practices have intensified alluvial and colluvial processes on much of the study area. Rock outcrops have been covered with spoil and detritus. Prospect pits and trenches have filled in with sediments. Treetops and branches scattered by current logging operations both limit access and screen outcrops. These factors have made structural inferences difficult. However, recurring road ditching has exposed previously covered beds, particularly the carbonate units.
VI. REGIONAL STRATIGRAPHY AND STRUCTURE
Hayes (1891, 1901) first discerned differences between rocks of the Paleozoic formations of the Ridge and Valley province and those of the Precambrian Blue Ridge province to the east. He mapped crystalline rocks east of the Great Smoky fault and Cambrian to Carboniferous sedimentary rocks west of the fault. Since Hayes' work the existence of the Great Smoky fault from the Pine Log Creek area northward into Tennessee has not been questioned, although its presence in the more southerly portions of the Cartersville Mining District has been the subject of controversy (Bentley, et al, 1966; Costello, et al, 1982; Kesler, 1950).
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The Great Smoky fault resulted from Paleozoic continental collision between proto-North America and proto-Euro-Africa and the island arcs that may have existed between them (Cook, Brown and Oliver, 1980). Recent deep seismic probes indicate the overthrust belt and the Paleozoic formations of the Ridge and Valley province are "thin-skinned" thrust stacks of sediments over an igneous and metamorphic "basement" (Hatcher, 1978). The total thickness of the Cambrian rocks in the Cartersville Mining District is in excess o 10,000 feet (3,048 meters) (Davis, 1984).
The Ridge and Valley province is characterized by faulted and folded formations of weakly metamorphosed Cambrian to Pennsylvanian sedimentary rocks. Folding and faulting is most intense adjacent to the Great Smoky fault and progressively decreases westward. Metamorphism of these sediments also is slightly higher grade in the east. Limbs of folds have steeper dip in the eastern portion of the province. Key tectonic features of the province are a master decollement above but near the "b asement" contact underlying rootless folds and moderate to steeply dipping thrust faults (Harris and Milici, 1977).
Deformation in the southern Appalachians occurred intermittently from the Ordovician to the Permian Periods (Higgins, 1984). Sediments probably accreted (to the depositional basin that has become the Ridge and Valley province) from both the North American and Euro-African continents (Eardley, 1951; King, 1950; Mack, 1980). Harris (1973) and Harris and Milici 0977) describe Cambrian to Lower Ordovician depositional environments in the province.
VII. LOCAL STRATIGRAPHY AND ROCK TYPES
Paleozoic formations in the study area have been named from type sections elsewhere in the Ridge and Valley province: the Chilhowee Group from exposures at Chilhowee, Tennessee; the Shady Dolomite from Shady Valley, Tennessee; the Rome Formation from the vicinity of Rome, Georgia; and the Conasauga Group from rocks along the Conasauga River in northwest Georgia. Thin-bedded carbonates in an inactive quarry a short distance east of the Great Smoky fault thrust front have been considered either as part of the Wilhite Formation of the Precambrian Ocoee Supergroup (Costello, et al, 1982) or a window of the Cambrian Conasauga Group (Cressler, et al, 1979) (Table 5).
Chilhowee Group (Weisner Formation)
Rocks of the Chilhowee Group are exposed along the Great Smoky fault in the eastern part of the study area. Dominant lithologies are arenaceous rocks composed of medium- to fine-grained, angular to wellrounded quartz grains. Some of the beds are arkosic. Other beds composed of rounded and frosted quartz grains suggest they were formed from both water and wind transported sediments.
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In the eastern one-third of the area arenites form weather-resistant ridges which have maximum elevation, within the study area, of 1305 feet (398 meters). Below this resistant unit the Chilhowee Group consists of alternating beds of sandstones, mudstones, thin shales which weather to a light-colored clay, and conglomerates. The latter three rock types occur only sparingly. The conglomerates and the sandstones vary in color from white to brown, gray, and maroon; some beds are highly ferruginous. Some thinner sandstone laminae are flexible. Thicker sandstone beds rarely show cross-bedding. Near the upper part of the sequence are occasional lenses of black phyllitic shale and silver gray graphitic shale. Mud cracks and ripple marks were not observed in situ but sometimes were observed in float. Extensive series of basal quartz pebble conglomeratic beds characteristic of the Weisner Formation (Mack, 1980) were not seen and therefore it is unlikely that the lower contact is exposed here.
The upper 27 feet (8 meters) of the Chilhowee, composed mainly of sandstones, is exposed in a abandoned flagstone quarry on East Valley Road adjacent to the Great Smoky fault. The bedding sequence is similar to that reported by Bentley, et al (1966) near White, Georgia and is typical of the upper portion of the group as described by Mack (1980). At both locations, "Pine Log" stone has been mined for many years. Other stone prospects have been tested throughout the exposed Chilhowee. Other outcrops of the group occur intermittently to 1.6 miles (2.6 km) west of the Great Smoky fault. Well borings show these sandstones extend easterly beneath the thrust for at least some distance. Float, prin~ipally of the more weather-resistant arenites, occurs in decreasing volume northwesterly down both Pine Log Creek and Sugar Hill Creek drainages.
Sporadic outcrops of the Chilhowee Group occur along the Great Smoky fault; from 0.25 mile (0.4 km) south of the junction of Bolivar and Falling Springs Roads, where an extensive bed of white sandstone is exposed near the head of a small valley, to the boulder fields along Pine Log Mountain and up the valleys adjacent Sugar Hill. Linear outcrops of blocky sandstone and weathered breccia mark the many fault zones in Chilhowee rocks. Because of extensive high-angle and thrust faulting stratigraphic thickness was not obtained; however, it is estimated to be at least 1000 feet (305 meters) thick (Mack, 1980).
Shady Dolomite
The Shady Dolomite conformably overlies the Chilhowee Group. Although no fossils were found in this study, Lower Cambrian archaeocycathids, brachiopods, trilobites and gastropods have been reported from the Shady (Butts and Gildersleeve, 1948; Chowns, 1977; Kesler, 1950).
The Shady Dolomite consists of four lithologies: dolostone, chert and jasperoid, a few shales and thin sandstones. Its contact with the Rome Formation is conformable and intergradational causing doubt about the exact demarcation between these two formations. Although much of the section is covered by alluvium, relations of the Shady to both the Chilhowee Group and Rome Formation can be observed.
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Dominant beds of the Shady Dolomite are dolostone and jasperoid: the dolostone is only slightly siliceous and eaSily weathered but jasperoid is erosion resistant. Jasperoid float overlies the Chilhowee Group quartzites at several places in the study area and is particularly common along and west of fault contacts between the Chilhowee and Shady.
Chowns (1977) and Cressler, et al (1979) estimated the Shady varied from 300-500 feet (92-152 meters) thick in the barite mining pits near Cartersville. McLemore and Hurst (1970) estimated its thickness at 1000 feet (305 meters).
Kesler (1950) considered the Shady dolostone to be only 30 feet (9 meters) thick and restricted to the manganese-hematite-barite zones immediately overlying Chilhowee quartzites. He considered the dolostone overlying the zone of interbedded hematite and dolomite to be the Rome limestone and dolomite in lenticular rather than continuous beds. He believed the Shady consisted of lenticular beds and identified the formation from its weathered ocherous and umberous clays and jasperoid.
Shady jasperoid varies from deep black to light yellow with anastomosing siliceous veins. Cressler, et al (1979) believed freshly broken Shady jasperoids are red, tan or brown, while Conasauga Group jasperoids are usually gray. Rome (of Kesler, 1950) jasperoids are brown. Jasperoids tend to be confined to Shady and Rome (of Kesler, 1950) dolostones: Conasauga and Knox Group carbonates west of the study area contain no jasperoid. Jasperoid is found in association with a barite-bearing dolostone, probably Shady, near Camp Ground Mountain, Eton, Georgia.
Croft (1963) believed the Shady Dolomite consisted of three main units: a lower unit of gray siliceous dolostone 300 feet (92 meters) thick; a middle unit of sandstone and shale 50-100 feet (15-30 meters) thick; and an upper unit of gray, sandy dolostone sometimes containing partings of shale. Croft indicated the latter forms jasperoid.
Table 1 compares the major oxide composition of the Shady, Rome (of Kesler, 1950), Conasauga carbonates and the Precambrian Wilhite Formation. In the Pine Log Creek area Shady dolostones are very homogeneous, differing significantly from carbonates of the other three formations, and most closely resembling Knox Group dolostones. Shady specimens from Pine Log Creek are almost identical in composition with those found in the Cartersville Mining District and other areas (Foote, 1984; Furcron, 1942; Kesler, 1950). Shady dolostones are only slightly siliceous; Rome carbonates, (of Kesler, 1950) are highly so. Analyses of Shady specimens reported by Kesler (1950, p.l3), which he considered Rome carbonates, are chemically similar to those considered Shady by Furcron and those collected in the Pine Log Creek study area (Foote, 1984). Kesler's numbers 14 and 18 appear to be Conasauga limestones and numbers 2 and 15 may be Rome Formation (of Kesler, 1950) carbonates. Kesler's sample number 18 is oolithic (Kesler, 1950, p.11), which is not characteristic of the Shady, and contains copper which has been reported within the Conasauga but not the Shady.
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In summarizing analyses of Shady carbonate rocks from 20 locations in the Cartersville district, Kesler (1950) concluded that the composition might be a stratigraphic feature, with the mineral dolomite being of sedimentary or diagenetic origin. "On the other hand, the lower beds are exposed only in the easterly outcrops, and the effects of metamorphism are increasingly apparent eastward ... 'so' it might be inferred ... that all the carbonate rocks were originally limestone, that magnesia was introduced during recrystallization, and that the more easterly rocks were more uniformly converted to dolomite than were those farther west .... the origin of the dolomite is not related to the deposition of ore minerals, for the content of magnesia shows no real relation to the mineral deposits .. 'the dolomite' is believed to be of premetamorphic origin, but there is no evidence to indicate whether it was precipitated directly in beds or was formed by reaction between limestone and sea water" (Kesler, 1950, p.l3).
Stuart (1956) suggested that the dolostone laminae in Conasauga carbonates near Fairmount were of primary origin, and that the secondary replacement of additional dolostone may have occurred after the rocks were deformed. Smith (1958) considered the Conasauga dolostones in the Ranger, Georgia area to be of diagenetic origin.
No modern dolomite deposits were kqown in 1950. Since 1965 modern dolomites have been recognized on Bonaire Island, Netherland Antilles; Andros Island, Bahamas; the Persian Gulf shore; Deep Spring Lake, California (Blatt, 1982); and Shark Bay, Australia (Harris, 1973). Magnesium-rich hypersaline brines are produced by evaporation in arid areas with low fresh water input and restricted sea water circulation, such as barred basins (Blatt, 1982; Jackson, 1970) and continental shelv~s (Harris, 1973). The dense brine sinks down into existing limestone where dolomitization occurs.
Croft (1963) may have included the Rome Formation carbonates (of Kesler, 1950) in the upper unit of his Shady Dolomite. As will be demonstrated, these carbonates intergrade with Rome Formation shales indicating penecontemporaneous deposition of the Shady Dolomite and Rome Formation.
The Shady Dolomite has been mined for brown iron ore, manganese, ocher and barite; abundant residual barite is diagnostic of the Shady (Butts and Gildersleeve, 1948).
Within the study area, Shady rocks have been thrust over the Rome Formation. The Rome Formation and Chilhowee Group thrust over the Shady Dolomite east of White, Georgia (Croft, 1963). Dolomite at Shinall Quarry in White, Georgia has similar composition to the Shady and crops out in the downthrown block of the White fault (Cressler, et al, 1979; McLemore and Hurst, 1970).
Rome Formation
The Rome Formation overlies the Shady Dolomite and is composed of sandstones, shales and carbonates. Croft (1963) estimated its thickness at 1500 feet (457 meters) but Cressler, et al (1979) and Chowns
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(1977) believed it to be 500 feet (152 meters) thick or less. Lower Cambrian fossils of Solenopleurella virginica Reeser, are reported by Butts and Gildersleeve (1948) from Rome Formation residuum immediately beneath overthrust Ocoee Supergroup phyllites. Similar fossil fragments were found by Cressler and this writer.
The Rome Formation contains some limestone lenses as well as a few beds of calcareous shale (Butts and Gildersleeve, 1948; Crawford, personal communication). Rome carbonates (of Kesler, 1950) are distinctive; except for the Conasauga Group these are the most highly siliceous carbonate rocks in the study area. They also contain higher concentrations of major oxides characteristic of Rome Formation shales
(Tables 1 & 2). The Rome carbonates (of Kesler, 1950) and the Rome metashales intergrade laterally. The Rome carbonate (of Kesler, 1950)
is a distinctive lithology: it can be mapped over some distance even though outcrops are dispersed and the bed has been faulted and weathered extensively.
Distinctive beds of the Rome Formation are the so-called "silver" shales. Visu~lly these shining shales are similar to the slightly duller Rogersville Shale of the Conasauga Group. Shearer (1918) noted the significantly higher potassium oxide content in the Rome shale, compared to the Rogersville, and this criterion was used to distinguish them (Table 3). Rome shales also contain greater amounts of magnesium oxide (Table 4).
Conasauga Group
The Conasauga Group is estimated to be 1500-4000 feet (457-1219 meters) thick (Butts and Gildersleeve, 1948). McLemore and Hurst (1970) divided the Conasauga Group into five major formations and the Pumpkin Valley Shale, a thin bed formerly considered to be part of the Rome Formation by some or the lowermost bed of the Conasauga Group by others. The Rome-Conasauga contact is conformable. To the west the Conasauga Group is overlain by the Cambrian-Ordovician Knox Group, which is not present in the study area.
The two major shale components of the Conasauga Group, Nolichucky and Rogersville Shales, are visually similar (Smith, 1958; Stuart, 1956) but only the latter occurs in the study area. The Rutledge Limestone in the Pine Log Creek area differs from carbonates of other formations here, a portion of one bed has been metamorphosed to a dolomitic marble. A few thin beds of metasiltstone occur in the Rogersville and the Rutledge.
The Conasauga Group underlies the western half of the study area, extending southwesterly from under the Great Smoky fault on Johnson Mountain. Sporadic thin beds of shale (Pumpkin Valley?) with sandstone interbe.ds occur above the Rome Formation and below the limestone (Rutledge Limestone?) of the Conasauga Group. The shale is rarely exposed. In the synclines along the White fault the shale has been overthrust by the Rome Formation.
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The Rutledge Limestone is light to dark gray, fine-grained crystalline limestone. Fractures, joints and bedding planes in fresh rock often possess a reddish cast. The Rutledge is 300 to 1000 feet (92-305 meters) thick (Chowns, 1970; McLemore and Hurst, 1970). Thin dolomitic layers on weathered surfaces mark the bedding planes on some Rutledge beds and may mark former algal growth during deposition. The Rutledge Limestone occasionally contains thin deposits of oolites, rare stylolites, and individual outcrops often are composed of highly siliceous rocks. Some limestone beds have been recrystallized and dolomitized. Brecciated zones contain much white calcite, particularly in contact zones with overlying Rogersville Shale. Partially weathered Rutledge Limestone occasionally contains copper minerals.
The Rutledge Limestone underlies valleys in the study area where it weathers to and is covered by dark terra rossa. Outcrops of the carbonate generally occur along the edges of hills where the Rutledge may form small scarps.
Hills in the study area consist of Rogersville Shale which is dull "silver" when fresh but weather to pink, maroon or brown fissile shale. The Rogersville is 1000 feet (305 meters) thick (McLemore and Hurst, 1970). Inter-bedded in the lower portion of the Rogersville Shale are somewhat sandy, gray metasiltstone laminae.
Upper Middle Cambrian trilobites were collected at Fairview Church and other nearby localities (Hurst and Crawford, 1970; McLemore and Hurst, 1970; Crawford, personal communication). C. Cressler collected Olenoides at Fairview Church and fragments of similar trilobites were collected at this location by McLemore and the writer. Pronounced cleavage of the shale has obliterated most fossils elsewhere in the study area but fragments occasionally are found. Some shale beds have been metamorphosed to phyllite and slate, which was extensively prospected in the past (Shearer, 1918). North of the study area, at Flexatile, Rogersville slate has been extensively quarried for roofing granule manufacture.
Two searches were made for conodonts and related fossils. Initially, 12.5 kg. (33.5 lbs.) of carbonate rock from Wilhite, Shady, Rome, and Rutledge outcrops disclosed a few phosphatic brachiopod fragments in samples from the Rutledge Limestone. The color alteration index of these fragments is 5 to 6, indicating the host rock reached a temperature of approximately 572 degrees F (300 degrees C). A second collection of 45.5 kg. (122 lbs.) of rock from 18 locations was negative for conodonts (Anita Harris, USGS, personal communication).
VIII. DEPOSITIONAL ENVIRONMENT
Harris and Milici (1977) and Harris (1973) have described the Cambrian to Lower Ordovician sedimentation of the Valley and Ridge province, and Blatt (1982) has suggested the processes by which dolomites originate. During Cambrian time the earth's equator occupied terrain along a line through present-day Texas and Minnesota (Blatt, 1982). During this time a transgressive sequence, from clastic to dominantly carbonate rock, was deposited 15-20 degrees south of the Cambrian equator along the edge of the North American craton. Continental drift has subsequently rotated these sediments to their present position.
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Initial Chilhowee Group (Mack, 1980) deposits of nearshore marine conglomerates, sandstones and shales were later - covered by Shady Dolomite which was deposited as a shallow carbonate bank. If deposited as a limestone, the Shady probably was penecontemporaneously dolomitized by pore fluids consisting of magnesium-rich brines (Blatt, 1982; Harris, 1973).
Deposition of the Shady Dolomite was accompanied by a period of variable energy and water level during which "terrigenous clastic rocks of the Rome Formation were deposited in an intertidal and shallow subtidal environment west of the Shady carbonate bank" (Harris and Milici, 1977). Sandstones, siltstones, shales and carbonates were deposited as periods of regression and transgression alternated, modifying the type and extent of the clastics deposited.
A period of basin subsidence leading to an offshore marine environment followed deposition of Rome rocks. The source of sediment during the Lower and Middle Cambrian was west and north; consequently deep-water lagoonal deposition of mostly fine-grained silt, shale and carbonates accumulated above and west of the Rome Formation (Harris and Milici, 1977). This sequence of Late Cambrian Conasauga limestones, shales and siltstones was supplanted by the Knox Group dolostones and limestones. The Knox Group, which extends from Canada to Mexico, was deposited in a saline subtidal system on the continental shelf (Harris, 1973). During the early Ordovician this wedge of sediments along the present-day eastern United States was uplifted: sedimentation ceased and a karst topography developed (Harris and Milici, 1977). Late Ordovician glaciation contributed to the lowered water levels.
The local environment when these sediments were deposited in the Pine Log Creek area probably was that of a quiet marine and fresh water embayment. A sandy beach front occupied the eastern edge of the study area behind which were a series of shallow pools of marine to brackish water. Variable water levels in the embayment periodically enlarged the beach front westward, so within the fluctuating littoral zone shallow pools were intermittently formed in which small amounts of carbonaceous matter was deposited. The beach front probably contained few dunes.
Seaward from the beach front, tidal flats existed periodically, their extent and location dependent upon water levels. Deeper waters west of the beach front were quiet during most of the depositional period. Most of the sediments deposited were fine-grained. Silt and larger particles occur more frequently in the Rome Formation which formed in shallower, less saline water. Sources of the sediments varied, producing beds of different composition in the four Paleozoic stratigraphic units (Eardley, 1951; King, 1950; Mack, 1980). During the Cambrian and Ordovician the waters were warm, the climate tropical, arid to sub-arid and the atmosphere perhaps contained slightly more carbon dioxide than at present. Blue-green, green, red and brown marine algae and calcareous megascopic algae were abundant. Animal life included archaeocyathids, brachiopods, molluscs and arthropods, like trilobites and related forms, which foraged _on the shallow sea bottom or burrowed into it.
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Evidence for this hypothesis on local conditions consists of the following:
1. Cross-bedding apppears to be uncommon, although exposures are limited;
2. Ripple marks are rare; ooliths occur sparingly in Conasauga carbonates in thin bands over short distances;
3. Graphitic phyllites occur interbedded with quartzites 1n the upper portion of the Chilhowee Group;
4. The four major stratigraphic units apparently are conformable to each other (Croft, 1963; Kesler, 1950);
5. No evidence was found of reef structures or aeolian sediments, although reef structures occur in the Cartersville Mining District (Crawford, personal communication);
6. During deposition of the Shady Dolomite, the environment may have been karst-like. Algae (crustose?) may have inhabited the calcitic muds leading to some dolomitization of carbonates deposited later, particularly along Conasauga Group bedding planes. Algae intercepted fine grained silica, which suggests water depths of 75 feet (23 meters) or less during most of the depositional period;
7. Predominance of shales and limestones and the life forms inhabiting them suggests a quiet, warm, shallow water environment punctuated briefly during deposition of the Rome Formation by lower water levels and deposition of larger particulate matter;
8. Relatively high magnesium content of Rome shales suggests the presence of algae;
9. Shale laminae are generally persistent and the shales contain few impurities, suggesting quiet water and sustained deposition.
IX. STRUCTURE
The Pine Log Creek area is a thrust stack of Paleozoic sediments underlain by a decollement and produced by thrusting from the southeast during a long period of recurrent deformation. As part of the Ridge and Valley province its structure is similar to that reported in Tennessee (Harris and Milici, 1977). Movement occurred principally along a major thrust fault above the basement-sediment contact. This low-angle thrust produced a series of northwestward movements in Chilhowee, Rome and Conasauga rocks. Kesler (1950) reports barite-bearing outcrops, probably of Shady dolostone, several miles west of White, Georgia.
11

Movement along major thrusts was uneven because different rock competencies were encountered, so many normal and' reverse faults were later formed to relieve the compression. Simultaneous imbrication of formations occurred differentially, changing stratigraphic order along the normal and reverse faults (Harris and Milici, 1977). Plate 1 shows the location of probable faults inferred from lithological and mineralogical evidence appearing on the surface. There are undoubtedly many other faults obscured by agriculture, forestry and tens of millions of years of weathering.
Doubly-plunging anticlines and synclines are dominant features of the Pine Log Creek area. Major first-generation thrusting produced a series of anticlines and synclines with an average strike of N30E. Subsequent folding resulted from compression directly from the south, produced doubly-plunging sequences along the first generation folds. Additional metamorphism formed multiple cleavages in the shales and recalcification of some carbonates. The direction of folding suggests the metamorphism may be related to formation of the Emerson (Cartersville) fault.
Orogenic effects on Pine Log Creek area appear superficially similar to those summarized by Bates (1968) for eastern Pennsylvania where Late Ordovician Taconic and Late Devonian Acadian thrusts from the southeast produced the dominant structure. Late Paleozoic thrusting from the south resulted in oblique cross-folding and probably the high-angle faults that were later mineralized. Higgins, et al (1984) have suggested the stacking of thrust sheets east of the Great Smoky fault in Georgia . :-occurred over a long period from the Ordovician through the Carboniferous.
Smith, Wampler and Green (1969) summarized isotopic dating (by Rb-Sr and K-Ar) and metamorphic isograds in Georgia crystalline rocks and concluded that cooling of the rocks after orogenies occurred over 350 million years ago in the northwest portion of the state. Radiometric specimens closest to the Pine Log Creek area were those from Fort Mountain, Tate and Allatoona Dam areas. The Acadian and Alleghenian orogenies produced the present low grade of metamorphism. Bentley, et al (1966) however, noted that two major periods of deformation were evident in the Corbin Gneiss and in the calcareous phyllites of the Shady Dolomite at the bull pasture outcrop.
Mack (1980) indicated Late Precambrian clastic sedimentation in the southern Appalachians began as a result of continental rifting. The taconic, Acadian and Alleghenian orogenies were the result of collisions between fragments of continents and island arcs at the eastern edge of proto-North America. Prior to 450-500 million years, sediments forming sandstones and shales of the Ridge and Valley province came from proto-North America. For the next 250 million years sediments came chiefly from land to the east, until disrupted by the Appalachian orogeny, 280-195 million years before the present (Cook, Brown and Oliver, 1980).
Kesler (1950) concluded the deformation occurred during the Carboniferous Period and could find no evidence of weaker prior deforma-
12

tion in the Cartersville Mining District. He wrote "faulting occurred near the close of folding .... and the occurrence nf brecciated barite enclosed in jasperoid shows that there was renewed movement along some of the faults after the barite had been deposited, and before the jasperoid had been deposited ... new faults were formed contemporaneously with further movement along those in which the ore materials had been deposited".
The absence of any significant recognized unconformities in the Pine Log Creek area and the similarities of folding and faulting in all four stratigraphic units suggests no orogenetic deformation occurred during deposition of the Chilhowee Group, Shady Dolomite, Rome Formation and the Conasauga Group. Nor are there reports of extensive sedimentary unconformities during this period elsewhere in the Ridge and Valley province.
Plunges of the folds vary from 5 degrees to more than 20 degrees; dominant directions are southwest and northeast. Some carbonates are skewed to nearly east-west orientations but most retain a dominant northeasterly strike. Shales and other less-competent beds were compressed and rotated to a more easterly strike so the beds are often slightly oblique to the more competent carbonate beds. The shales veer to the northeast, often accompanied by shearing, evidence of multiple cleavages and minor faulting. Some carbonate beds were thrust-faulted adjacent to shales and fault zones are marked by calcite in the cleavage planes of the shales. Drag folds are common in the shales. Some carbonate beds show partings, usually on the bedding planes. Fault zones of great extent occur throughout the study area as evidenced by brecciation, mineralization, limited gouge, slickensides and alignment of springs and sinks. Such zones are more abundant in the eastern than in the western parts of the study area.
Jointing in all of the formations is predominantly northwesterly; the drainage pattern closely follows fractures related to the joints.
Mineralization and silicification of carbonate rocks is most pronounced in the easternmost carbonates and decreases westward.
Most mineralization is the result of post-metamorphic weathering and introduction of hydrothermal fluids. Dolomitization occurred prior to mineralization as Kesler (1950) indicated; mineralization occurs at high-angle faults, some of which cross-cut the dominant structures and therefore are of later origin. Mineralized solutions moved northwestward along joints and faults: if a significant sulfide ore body is present, it may be located in the Sugar Hill area, southeast of the 6 confirmed sulfide shows and the alluvial sulfide densities denoted by Hurst and Crawford (1970).
Although now eroded away, the front of the Great Smoky overthrust may originally have extended westward nearly to U.S. Highway 411. Paleozoic formations extend eastward under the crystalline rocks for some distance and are encountered in well borings. A massive housesized block of quartzite occurs in the Rome Formation outcrop 0.25 mile (0.4 kilometer) west of hill 1305 suggesting the Chilhowee was thrust at least this far west of its present position. No relics of postCambrian Paleozoic rocks were found in the study area.
13

Between the bull pasture Shady Dolomite outcrop and the Sugar Hill Creek ford outcrop (Plate 1 and Figure 1) much Shady jasperoid appears on the surface above Rome shales. The area is mineralized and reappearance of the Shady at the Sugar Hill Creek ford probably is due to overthrusting and faulting; the Shady was transported a considerable distance across Rome shales.
While most beds dip to the southeast from 10 to 40 degrees, a few dip to the northwest; some can be paired as opposing limbs of small anticlines or synclines. At contacts between shales and more competent beds, dips on the shale cleavages generally increase; some beds are vertical or nearly so.
X. STRUCTURE OF INDIVIDUAL FORMATIONS
Chilhowee Group
The Chilhowee Group formed along an interrupted anticlinorium (Kesler, 1950) extending from Tennessee to south of Cartersville where it is overthrust by rocks of the Emerson fault. For part of this distance the Chilhowee has been overthrust by the Ocoee thrust sheet; where exposed, it has been compressed into a series of thrust faults, high-angle faults and folds.
Exposures of 11 dirty11 quartzites of undetermined or1g1n crop out in a few places within the Ocoee Supergroup east of the Great Smoky fault. Whether or not these outcrops are protrusions of Chilhowee rocks exposed by weathering is unknown. One outcrop has been traced more than 300 feet (100 meters) west of the carbonate quarry and other small occurrences have been noted by C. Cressler (personal communication).
At the southeastern border of the study area the Chilhowee disappears under the boulder fields descending from Pine Log Mountain and here the Chilhowee's relation to the Great Smoky and Pine Log Mountain fault (Cressler, et. al, 1979) is obscure. In the northeastern portion of the study area Ocoee-Chilhowee contacts also have been obscured by alluvium from the overthrust sheet; along stone quarries at the eastern edge of the area the two formations are in close proximity, and the contact is marked by a change in lithology over a few meters distance.
Throughout the eastern portion of the study area the Chilhowee forms a series of disconnected ridges consisting of two prominent anticlines, separated by a fault, with steeper west-facing declivities. On the downthrown side of such faults, erosion-resistant quartzite boulders form taluses. Slickensides are common structural features and shaly beds of mixed quartzite, sandstone and muscovite have been phyllitized.
Dips of the formation are predominantly southeastward and vary from nearly horizontal to almost vertical. Rocks adjacent to the Ocoee overthrust sheet usually dip from 18 to 30 degrees and strike N20-30E.

From the contact with Ocoee rocks westward to the top of hill 1305 small scattered areas containing mineralized float suggest Shady dolostones previously occurred over the Chilhowee quartzite this close to the Ocoee overthrust. According to the landowner, a well was drilled in 147 feet (45 meters) of Ocoee phyllites and 198 feet (60 meters) of quartzites to reach a total depth of 345 feet (105 meters). This well is located 210 yards (192 meters) east of the front of the overthrust sheet, near a residence on East Valley Road 0.9 miles (1.4 km) south of Georgia Highway 140. Well borings did not react to acid so carbonates probably were not encountered in the bored section.
Thrust faulting within the Chilhowee is marked by conspicuous lines of brecciated quartzite cemented with limonite. Faults occur in all the stone quarries; competent quartzites have been thrust over shale beds and the faults are exposed in the quarry faces.
In summary, the Chilhowee was thrust westward into two prominent and many minor fault-separated anticlines; subsequent crustal shortening produced high-angle faults and folds of lesser magnitude parallel and oblique to the initial strike axis.
Shady Dolomite
The Shady Dolomite consists of one bed of dolostones approximately 100 feet (30 meters) thick and a small amount of shales and sandstones. These beds conformably overlie Chilhowee Group quartzites. Jasperoid, probably formed by hydrothermal introduction of silicates, occurs in beds, lenticular outcrops and float: usually it is associated with dolomite. Post-silicification mineralization (Kesler, 1950) of the carbonates, particularly along fault zones, produced lines of float of boulder- to granule-sized manganese-hematite-barite nodules: where abundant this mineralization marks the former distribution of the carbonate.
Southeast of the Chilhowee-Shady contact at Seven Springs, the Shady forms a small north-facing scarp on Oak Hill. Other Shady exposures occur on hill 1305 above the Chilhowee and between Chilhowee faults, at the bull pasture, in the valley between Sugar Hill and Pine Log Mountain, on the southeast side of South Hill, and at Sugar Hill Creek ford. The Shady appears in a small outcrop south of the Bolivar Road, Rome fossil site as previously noted by Kesler (1950, p. 13, No. 20) and Croft (1963). A carbonate equivalent to the Shady outcrops on Bolivar Road at a ditch bridge one-half mile east of U.S. Highway 411. Usually the Shady is associated with jasperoid which often occurs northwestward of the fresh rock. Kesler (1950) also reported that jasperoid and manganese-iron-barite mineral zones are characteristic of the Shady. Other jasperoid occurrences are scattered throughout the study area.
Two exposures of the Shady along Pine Log Creek are thrust-faulted sections of the same bed; between these outcrops are Chilhowee shales and sandstones. Across the east side of nearby Oak Hill the same Shady bed is nearly intact and horizontally bedded; on the west side of the hill, Shady overrides Rome Formation shales.
15

At the bull pasture the Shady is faulted against Rome shales; it reappears near Sugar Hill Creek ford again overlying Rome shales. Parallel to the creek some 660 feet (200 meters) north the area between the bull pasture and ford is marked by an abundance of mineralized jasperoid float, some of which has been prospected by churn drilling, apparently for sulfides, iron or manganese minerals.
Most Shady Dolomite beds dip to the southeast. Drag folds are uncommon, but two observed on Oak Hill suggest the bed here was plunging to the southwest. Because the Shady was thrust over Rome shales for varying distances, the initial contact between these formations has long been in doubt. Along Pine Log Creek the Shady-Rome contact occurs downstream from Seven Springs.
Several rock specimens collected in a ditch on Bolivar Road are identical to other Shady dolostones. West of this outcrop a ConasaugaRutledge Formation anticline, accompanied by silicate rich beds, extends east from U.S. Highway 411. A second faulted Shady outcrop is 492 feet (150 meters) north of the two large shale hills through which
Pine Log Creek has cut. An iron-manganese zone, oblique to the major
strike axis and nearby conglomerates, may indicate a high-angle fault here. It is probable the Shady dolostone was ramped upward and to the west to lie against the competent Rutledge; the eastern contact of the Shady here penetrated shales which may be part of the Rome Formation.
Rome Formation
Rome sandstones are the major lithology along the White fault (Cressler, et al, 1979). Sugar Hill Road crosses the fault where the hard brown Rome sandstone was thrown upward to form the southeast end of a northeast-trending ridge. The faulted and broken sandstone underlies the ridge west of Pleasant Olive Church where it has been prospected for building stone. Along the east flank of this low ridge, Rome shales have been imbricated onto the sandstone so the two lithologies appear to obliquely alternate. The less competent beds tend to curve more to the northeast and are oblique to the strike of the sandstones.
Thickness of the Rome Formation is estimated at about 950 feet (290 meters). Rome Formation contains a single dolostone bed which is repeated by faulting. Sandstones and shales appear between the west exposure of Shady dolostone and again between the east and west outcrops of the Rome dolostone. Hard sandstone, in contact with the west outcrop of Rome dolostone, is faulted with the dolostone and forms the ridge- forming sandstone previously discussed. North of Sugar Hill Creek ford the Rome dolostone-sandstone combination has been offset to the northwest, suggesting a strike slip or high angle fault.
Outcrops of imbricated Rome (of Kesler, 1950) and Shady carbonates occur west of the White fault and are marked on Plate 1. Kesler (1950) believed these carbonates could be identified by the presence of hematite-manganese-barite mineralization. Analyses of the composition of several specimens also suggests the surface exposure of the two lithologies west of the White fault. The evidence, however, is not conclusive. (Plate 1; Kesler, 1950; Foote, 1984).
16

Rome "silver" shales were extensively prospected for potash. Two notable prospects were cuts, several hundred feet wide, across the strike west of Oak Hill. With allowances for the major fault that underlies the beds, the shales here may be as much as 400 feet (122 meters) thick. Elsewhere there are many small test pits in both Rome and Rogersville shales made during and after World War I when supplies of potash became unavailable from Europe. Rogersville slates formerly mined at nearby Flexatile were used in roofing and flooring products and as an inert additive to fertilizers.
Tables 1 and 4 consider major oxides content and differences in compositional variability of major oxides in the four carbonates. The data suggests, but does not conclusively prove, that the carbonate samples Wl, W2, and W3 are part of the Rome Formation (of Kesler, 1950) (Table 5).
Conasauga Group
In the Pine Log study area the Conasauga Group comprises three Formations: Pumpkin Valley Shale, Rutledge Limestone and Rogersville Shale. Pumpkin Valley Shale may crop out between Rome sandstones and Rutledge limestones. Two possible exposures were noted: 1) immediately south of the Wesley Smith Farm where a small shale anticline occurs; and 2) on the hill west of Oak Hill Church, west of Falling Springs Road along the White fault.
The White fault crosses the paved county highway south of the Sugar Hill Road where large amounts of Rome sandstone brecciation appear. The fault crosses the latter road and is marked by a steeply-dipping blocky sandstone bed. Shales east of the sandstone are Rome; those west of the fault zone are Rogersville. The contact is obscured by alluvium. Between the Sugar Hill Road and the Vaughn Dairy Road, the White fault follows the western edge of the Rome sandstone ridge.
The Rutledge Limestone appears regularly on the southwest and northeast of hills covered by Rogersville Shale throughout the western portion of the study area. East of Fairview Church, north of Georgia Highway 140, the Rutledge forms a long doubly-plunging anticline with a small erosional scarp on the west limb.
Between Vaughn Dairy Road and Georgia Highway 140 the White fault becomes more sinuous and is obscured by overthrusting of Rome sandstones and shale; these curving thrusts are apparent on aerial maps. The zone is well marked with a substantial sink in Rutledge Limestone on the west side of the hill. At Sugar Hill Creek, the Rutledge has been thrust to near vertical. The White fault crosses Georgia Highway 140 about 492 feet (150 meters) east of the Knucklesville Road junction; from there it curves easterly and probably crosses Pine Log Creek west of the Falling Springs Road bridge. Croft's (1963) map suggests the fault occurs upstream a short distance east of the bridge but Rome carbonates (of Kesler, 1950) and sandstones both west and north make it more likely the fault occurs downstream.
17

North of Georgia Highway 140, the Rutledge , has been folded and faulted into curving and plunging beds. Rogersville Shale beds sometimes are continued across the folds of plunging synclines. Considerable local thrusting occurred: white crystallized calcite interfingers with the shale beds at points of contact; springs and sinks are numerous; one of significant extent may be called a cavern.
XI. WATER RESOURCES.
The Pine Log Creek area contains an abundant supply of high quality ground water (Cressler, et al, 1979). Locations of springs are shown on Plate 1. While much of the local aquifer recharge results from rain falling on the area, some probably originates elsewhere. Discharges from three major springs - Seven Springs, Oak Hill Church Spring and U.S. Highway 411 Spring - amount to nearly 8% of the estimated average annual rainfall on the 14 square mile (36 square km) study area. Many other springs discharge 10,000 gallons (37,800 liters) or more per day. All the springs are related to carbonates of the Shady, Rome (of Kesler, 1950) and Rutledge formations. The springs occur at fracture, joint, dissdlution zones in the carbonates, and at shale-carbonate contacts.
The spring under U.S. Highway 411 contained a weir and its flow was periodically monitored during 1981 and 1982. Despite a prolonged drought during the summer of 1981, said to be the worst locally since 1925, little fluctuation occurred in the spring's discharge of 610,000 gallons (2.3 million liters) per day. No obvious fluctuation was apparent in outflow of either the Oak Hill Church spring, estimated at 1,000,000 gallons (3.8 million liters) per day (Cressler, et al, 1979) or the Seven Springs spring, which Cressler estimated to yield 750,000 gallons (2.8 million liters) per day (personal communication). The U.S. Highway 411 spring has recently been developed by Bartow County to supply water to the village of Pine Log and adjacent regions.
Water from the Oak Hill Church spring contains higher than usual amounts of potassium and magnesium, possibly because it emerges at the contact of Rome (of Kesler, 1950) dolostone and Rome "silver" shales: the latter contains significant amounts of potassium and magnesium. Both spring and well water from the Pine Log Creek area are alkaline with a pH varying from 7.2-7.7. Domestic and agricultural supply wells range in depth from as little as 6 feet (2 meters) to more than 200 feet (61 meters) and usually provide from 5 to 20 gallons (19 to 76 liters) per minute. Before the consolidation of land ownership the Pine Log area consisted of many small farms and abandoned wells are numerous. Most of these wells apparently were dug by hand close to the family dwelling, an indication of the abundance of ground water and the ease with which it was obtained.
Surface water of Pine Log and Sugar Hill Creeks remained plentiful during the 1981 drought due to the sustained ground-water flow; both creeks have supplied irrigation water for improved haylands during the last four grow1ng seasons. This use is expected to increase in the future.
18 '

A Corning Model 3 meter was used to determine water pH for a profile of Pine Log Creek from its headwaters to U,S. Highway 411. Winter pH of tributary waters from the south, those draining the north slopes of Pine Log Mountain, ranged from 6.3-6.8; water from one north-draining tributary from the upper beds of the Ocoee overthrust was more acidic, pH 5.3. In the area immediately east of the Great Smoky overthrust, tributaries draining the Wilhite outcrops ranged in pH from 7.2-7.5. A spring north of the study area and east of Falling Springs Road measured 7.2 and this water disappeared in a sink approximately 330 feet (100 meters) west of the overthrust contact. The pH of other spring waters are: Seven Springs, 7.7; Oak Hill Church Spring, 7.6; U.S. Highway 411 Spring, 7.3.
Results of this survey suggest carbonates occur in the lower beds of the Ocoee Supergroup for some distance east of the Great Smoky fault as previously noted by Smith (1959) and may be close to the surface
along the Pine Log Mountain fault. An alternate explanation is that
Cambrian carbonates, including the "Wilhite" quarry dolostone, underlie the overthrust for some distance easterly. Both Ocoee and Paleozoic carbonates may be present since Ocoee carbonates described by Smith (1959) occur as linear laminae a few centimeters thick interbedded with shales, while the quarry dolostone is a massive, relatively homogeneous block occupying several acres.
False gossans occur in Pine Log Creek and may suggest hidden contact or fault zones of Shady-Chilhowee rocks. The fresh water periwinkle mollusk is a positive indicator of alkaline waters; its abundance in Pine Log Creek in riffles varies with the alkalinity or acidity of its immediate habitat.
XII. MINERAL RESOURCES
Mineral resources of the Pine Log Creek area were first described in 1918. The first report consisted of records of potassium in Rome shales and utility of Rogersville Shale for building slate (Shearer, 1918). Mining activity and estimates of tonnages of brown iron and manganese ores produced (Kesler, 1950), prospects for use of carbonates for cement and road building materials (McLemore and Hurst, 1970) and surveys of copper and zinc (Hurst and Crawford, 1970) have been discussed in later reports.
Collections of shale specimens made during this study, some of which were from locations carefully described by Shearer (1918), duplicated the latter's results, although concentrations of potassium were slightly less (Figure 1 and Table 2).
Collections of iron and manganese specimens made during this study disclosed several additional outcrops not reported by Kesler (1950). Their locations are given in Figure 1 and their composition is summarized in Table 6. A special search was made for cobalt and low concentrations were found in two locations on the study area and on other localities in the Cartersville Mining District. Results can be compared with those of Pierce (1944).
19

Although barite has been mined in the District for many years none was found in the study area during careful searches, including collections of alluvium weathering from Shady and Rome (of Kesler, 1950) carbonate beds and alluvial samples of heavy minerals from natural sluices in Pine Log and Sugar Hill Creeks.
As one means of identification of carbonates, major element analyses were made on 55 specimens. Collection localities appear on Figure 1. Sulfide shows were found at three locations in addition to the two reported by Kesler (1950) and Cressler, et al (1979). All were in Rutledge Limestone and contained small amounts of gold and silver as well as copper. If a sulfide ore body of significance exists, it probably occurs east and south of the study area because the ions probably moved north and west along northwest-trending faults and joints.
20

Figure 1. - Sample locations and place names in Pine Log Creek map area
.21

Table 1. Percentage of major oxides in specimens of carbonate rocks of Rutledge Limestone (Conasauga Group), Rome Formation (of Kesler, 1950), Shady Dolomite and Wilhite Formation.

RUTLEDGE LIWESTONE (Conasauga Group)

7

14 17 20 27 B2A C1 C2 C3 1Y

AS1i02o23

3.63 0.96

5.74 0.95

0.81 0.22

6.92 2.01

2.28 0.78

6.60 3.50

4.12 1. 60

6.74 2.30

2.94 1. 80

0. 72 2.80

MgO 1.04 2.90 2.34 2.82 1.29 3.27 7.20 6.40 6.00 3.30

Fe2o3 1.22 0.61 0.30 0.91 0.39 1.30 0.95 1.40 0.50 0.40 CaO 52.6 52.7 57.2 41.7 51.9 40.4 43.7 42.3 45.9 49.16

K20

-

-

-

-

-

- 0.20 0.40 0.15 0.0

Total 59.45 62.90 60.87 54.36 56.64 55.07 57.77 59.54 57.29 56.38

SHADY DOLOMITE

1

5

6

8

15 18 19 22 23 24 25

3X

N

N

Si0 2 0.82 0 . 80 4.52 0.79 1.87 9.93 3.84 5. 72 3.34 7.61 7.57 0.34

A1 2o3 o.45 0.48 1.14 0.11 0.10 2.26 0.11 1. 99 1.12 0. 74 0.84 3.00

MgO 21.9 21.0 20.1 21.9 20.9 19.6 20.0 19.2 20.2 19.6 19.2 20.40

Fe2o3 0.86 1.49 1.59 1.52 1.12 2.06 2.19 1.42 2.23 0.58 1.66 1.20

CaO 30.6 31.2 30.1 32.2 29.1 28.5 29.0 27.3 28.8 29.7 28.7 28.00

K20

-

-

-

-

-

-

-

-

-

-

- 0.00

Total 54.63 54.97 57.45 56.52 53.09 62.35 55.14 55.63 55.69 58.23 57.97(46.72=LIG)

SHADY (Cont.) 31 32 S1 S2 S3 S4 S6 S7 B1 B2B B31

Si0 2 0.20 1.20 5.20 2.42 1.80 3.80 0. 72 4.94 6.8 9.0 2.0 A1 2o3 1.73 0.26 5.70 5.80 3.90 2.50 0.80 0.70 0.42 0.67 0.82 MgO 19.4 21.2 18.5 19.7 20.9 21.0 22.0 20.6 18.2 17.90 18.40
Fe2o3 1.34 0.36 0.40 1.00 0.95 1.40 0.75 0.95 1. 87 1.49 1.38
CaO 28.0 29.8 27.80 27.90 28.0 27.4 29.0 28.0 27.2 27.7 29.2 K20 Total 50.67 52.82 57.60 56.82 55.55 56.10 53.27 55.19 54.49 56.76 51.80

Table 1 (Cont.)

ROME FORMATION (of Kesler, 1950)

lX

85

2X

4X

5X

6X

7X

8X

30

9

8i02 Al203 MgO
Fe203 CaO
K20 Total

21.82 2.50
15.30 1.45
21.00 1.00
63.07

11.60 1. 20
18.50 1.25
25.50 0.80
58.85

40.00 9.40 7.30 2.20
15.60 1.80
76.30

23.46 8.20
12.80 2.90
19.00 1.50
67.86

50.00 18 .40 4.90
2.00 5.60 2.20 83.10

29.90 4. 70 3.26 2.80
26.88 1.50
69.04

22.14 11.00 13.00
1. 70 20.16
1.10 69.10

51.80 12.00
1.64 1.30 15.68 2.20 84.62

43.90 6.70 1. 30 3.14
23.50
78.54

27.00 0.29 0.29 5.13
21.70
54.41

ROME (Cont.)

10

11

12

13

16

21

8102 67.80 7.43 14.10 42.60 40.40 13.40

w N

A1203 7.34 3.87 2.66 10.10 8.15 2.86

MgO

0.76 17.70 3.02 7.34 0.20 0.34

Fe2o3 2.07 2.62 1.16 3.12 2.83 2.06

CaO

7.56 27.10 44.20 11.40 14.70 24.80

K20 Total 85.53 58.72 65.14 74.56 66.28 43.46

WILHITE FORMATION

2

3

4

26

W1

W2

W3

8102
A1 2o3
MgO
Fe 2o3
CaO
K20
Total

25.4 5.92 0.75 1.43
36.5
-
70.00

49.0 1.12 0.23 1.33
15.5
-
67.18

16.4 0.51 0.33 2.39
24.3
-
43.93

29.5 10.5
0.19
3.82 19.4
-
63.41

26.54 4.0 5.20 1. 70 29.0 0.60 67.04

57.26 7.0 0.90 3.20
15.68 1.50
85.54

18.52 3.9 1. 70 1.20
39.20 0.80 65.32

Table 1, (Cont.)

Mean and standard deviation of percentages of major oxides of Rutledge Limestone (Conasauga), Shady Dolomite, Rome Formation (of Kesler, 1950) and Wilhite Formation carbonates from the Pine Log Creek study area. Note similarities between Rome and Wilhite in average content and variability.

OXIDE

CONASAUGA SHADY ROME WILHITE

10

22

16

7

Si02

Mean

4.05 3.86 31.71 31.80

St.Dev. 2.38 2.92 17.08 15.44

A1203 Mean

1.69 1.48 6.84 4. 71

St.Dev. 1.00 1.66 4.75 3.46

MgO

Mean

3.66 20.06 6.73 1.33

N
+:--

St .Dev. 2.14 1.22 6.60 l. 79

Fe203 Mean

0.80 1.30 2.42 2.14

St .Dev. .412

.53 1.00 1.04

CaO

Mean

47.76 28.87 20.27 25.65

St .Dev. 5.74 1. 31 9.15 9.63

All chemical analyses were performed by Rocky Mountain Geochemical Corp., West Jordan, Utah. All analyses determined by atomic absorption.
Collection locations are shown on Figure 1.

Table 2. Chemical analyses of shale samples, Pine Log Creek Area.

%
AFS1ei022oo233
MgO CaO
Na 2o
K20
Ti02 MnO P2os L.Ig

ls 60.30 21.40
7.20 1. so 8.30 0.70 3.20 0.80 0. 02 o.os 4 . S2

ROGERSVILLE SHALE

13s

14s 4s

49.16 S6.40 S9.40

29.30 20.88 18.20

9.80 9.60 10.20

0.70 1.10 2.10

0.10 0.20 0.20

0.90 0.9S O.lS

3.10 4.SO 2.90

0.96 0.88 0.90

0.08 0.03 0.01

0.00 0.02 0.02

S.80 S.40 S.90

lSs S7.SO 21.70
8.40 1. so 0.20 0.20 3.80 0 . 7S 0 . 03 o.os S.77

6s S4.90 24.SO 10.10
0.40 0.10 0.60 3.40 0.60 0.01 0.05 S.32

8s S2.40 26.20
9.80 1. 60 0.30 0.60 2.90 0.60 0.10 0.02 S.43

TOTAL:

99.69 99.90 99.94 99.98 97.98 99.98 99.9S

AFS1ei022o2o33
MgO CaO Na 2o K2 0 Ti02 MnO
P2os L.Ig.

7s S9.74 21.80
S.lO 3. 30 0.20 0. 20 4.60 0. 77 0 . 06 0.05 4.16

ROME FORMATION

Ss

9s lOs

SS.24 S0.70 SS.83

23.30 29.40 22.20

7.80 6.70 7.80

3.SO 0.60 3.40

0.30 0 . 10 0.30

o.os 0.80 0.04

S.20 4. 90 S.90

0. 77 1. 04 0.68

0.02 0.00 0.01

0.01 0.02 0.00

3. 77 S.60 3.7S

lls 6S.OO 18.00
4.20 3.60 0.30 0.04
5.10 0.68 0.00 0.05 3.10

12s 68.28 16.80 4. 30
1. 70 0.20 0.10 4.80 0.68 0.1S 0.02 2.84

TOTAL:

99.98 99.96 99.86 99.91 100.07 99.87

Si02 A1 2o3 Fe 2o 3 MgO CaO Na 2o K20 Ti02 MnO
P2os L.Ig.

ROME FORMATION

2s

3s

16s

62.88 64.60 66.76

18.40 19.SO 14.90

S.80 4.90 S.90

3.40 1.40 3.20

0.40 0.30 0.30

8 . 10 o.os o.os

S.lO 4.80 S.80

0.60 0. 77 0.7S

0.00 0.00 0.01

0.00 0.02 0.02

3.30 3.92 2.24

TOTAL:

107.98 100.26 99.93

L.Ig. = Loss on Ignition

2S

Table 3. Percent potassium oxide in Rome Formation and Conasauga Group, Rogersville Shale.

Specimen No. Rome

Specimen No. Rogersville

2

5.1

4

2.9

5

5.2

8

2.9

7*

4.6

1

3.2

10

5.9

6**

3.4

11

5.1

13

3.1

12

4.8

14

4. 5

16

5.8

15

3.8

3

4.8

9

4.9

Mean 5.1

Mean 3.4

* Collected at Rome fossil site, Bolivar Road. ** Collected at Rogersville fossil site, Fairview Church.
t=6.78, calculated value. t.01-4.14 table value. The difference is highly significant.

Table 4. Percent magnesium oxide in Rome Formation (of Kesler, 1950) and Conasauga Group, Rogersville Shale.

Specimen No. Rome

Specimen No.

Rogersville

2

3.4

1

1.5

3

1.4

4

2.1

5

3.5

6**

0.4

7*

3.3

8

1.6

9

0.6

13

0.7

10

3.4

14

1.1

11

3.5

15

1.5

12

1.7

16

3.2

Mean 2.66

Mean 1.27

* Collected at Rome fossil site, Bolivar Road. ** Collected at Rogersville fossil site, Fairview Church.
t=2.97, calculated value. t.10=2.97 table value. The difference is significant.

Figure 1 shows specimen locations.

26

Table 5.

Results of Duncan Multiple Range Test for differences of mean percentage of major oxides in Rutledge( C) (conasauga), Rome (R), Shady (S) and Wilhite (W) carbonates in the Pine Log Creek Area.

Carbonates Si0 2

C-R

sig.

c-w

Sl.g.

c-s

NOT

S-R

sig.

s-w

Sl.g.

W-R

NOT

A1 2o3
Slg. NOT NOT sig. NOT NOT

Oxides

MgO

Fe 2o3 CaO

NOT

Sl.g.

sig.

NOT

Sl.g.

sig.

sig

NOT

Slg.

Slg. sig.

sig.

sig. NOT

NOT

sig. NOT

NOT

Note: Alpha = 0.01
sig. = significant
NOT = not significant
(after Kramer, 1956)

Table 6. Analyses of other elements in carbonates.

Element B3-2

Specimen Number

B-4

81-62 81-63 LEF-2

oz/T Gold oz/T Silver ppm Copper ppm Cobalt ppm Nickel ppm Lead ppm Zinc ppm Manganese %Iron Sulfide

-.003 -.03
0.13 -5 -5 10 5 675
0.97

-.003 0.02

-.03

0.01

5

0.80

-5

-5

30

5

375

21

1.4

30

0.50

14.80 23

ppm Cobalt ppm Nickel

Specimen Number

3/28

3/30

.099

.198

.781

.543

A minus sign (-) is to be read "less than". oz/T is to be read "Troy ounce per ton".
See Figure 1 for sample locations.

27

LITERATURE CITED
Adams, J.E. and Rhodes, M.L., 1960, Dolomitization by seepage refluxion: American Association of Petroleum Geologists Bulletin, v. 44, p. 1912-1920.
Bates, R.L., 1968, Geology of Industrial Rocks and Minerals: New York, Dover Publications, 459 p.
Bentley, R.D., Fairley, W.M., Fields, H.H., Power, W.R. and Smith, J.W., 1966, The Cartersville fault problem: Gerogia Geologic Survey Guidebook 4, 38 p.
Billings, M.P., 1954, Structural Geology: Englewood Cliffs, N.J., Prentice-Hall, 514 p.
Blatt, H., 1982, Sedimentary Petrology: San Francisco, H.W. Freeman and Co., 514 p.
Butts, C. and Gildersleeve, B., 1948, Geology and Mineral Resources of the Paleozoic Area in Northwest Georgia: Georgia Geologic Survey Bulletin 54, 176 p.
Chowns, T.M., 1977, Stratigraphy and Economic Geology of Cambrian and Ordovician Rocks in Bartow and Polk Counties, Georgia: Georgia Geologic Survey Guidebook 16-A, 21 p.
Compton, R.R., 1962, Manual of Field Geology: New York, John Wiley and Sons, 378 p.
Cook, F.A., 1983, Some consequences of palinspastic reconstruction in the southern Appalachians: Geology, v. 11, n. 2, p. 86-89
Cook, F.A., Brown, L.D., and Oliver, J.E., 1980, The southern Appalachians and the growth of continents: Scientific American, v. 243, n. 4, p. 156-158.
Costello, J.O., McConnell, K.I., and Power, W. R., 1982, Geology of Late Precambrian and Early Paleozoic rocks in and near the Cartersville District Georgia: 17th Annual Field Trip, Georgia Geological Society, 40 p.
Cressler, C.W., 1974, Geology and Ground-water Resources of Gordon, Whitfield and Murray Counties, Georgia: Georgia Geologic Survey Information Circular 47, 56 p.
Cressler, C.W., Franklin, M.A. and Hester, W.G., 1976, Availability of Water Supplies in Northwest Georgia: Georgia Geologic Survey Bulletin 91, 56 p.
Cressler, C.W., Blanchard, Jr., H.E., and Hester, W.G., 1979, Geohydrology of Bartow, Cherokee and Forsyth Counties, Georgia: Georgia Geologic Survey Information Circular 50, 45 p.
28

Croft, M.G., 1963, Geology and Ground-water Resources of Bartow County, Georgia: U.S. Geological Survey Water Supply Paper 1619-FF, 32 p.
Davis, K.R., 1984, Cartersville Geologic Section, in Arora, R., Ed., Hydrogeologic evaluation for underground injection control in North Georgia: Georgia Geologic Survey Hydrologic Atlas 12.
Eardley, A.J., 1951, Structural Geology of North America: New York, Harper Brothers, 624 p.
Foote, L.E., 1984, Major-element analyses; an aid to differentiating Early Paleozoic Great Valley carbonates: Georgia Geologic Survey Open-File Report 85-4, 7 p., 13 tables.
Furcron, A.S., 1942, Dolomites and Magnesium Limestones in Georgia: Georgia Geologic Survey Information Circular 14, 30 p.
Goff, J.H., 1963, Short Studies of Georgia Place Names. No. 91: Georgia Mineral News-Letter, v. 16, n. 1-2, p. 45-47.
Harris, L.D., 1973, Dolomitization model for Upper Cambrian and Lower Ordovician carbonate rocks in the eastern United States. U.S. Geological Survey Journal of Research, v. 1, n. 1, p. 63-78.
Harris, L.D., and Milici, R.C., 1977, Characteristics of thin-skinned style of deformation in the southern Appalachians and potential hydrocarbon traps: U.S. Geological Survey Professional Paper 1018, 40 p.
Hatcher, R.D., Jr., 1978, Tectonics of the Western Piedmont and Blue Ridge, Southern Appalachians: Review and Speculation. American Journal of Science, v. 278, p. 276-304.
Hayes, C.W., 1891, The overthrust faults of the southern Appalachians. Geological Society of America Bulletin, v. 2, p. 141-154.
, 1901, Geological Relations of the iron-ores 1.n the ----:C::a-r-t-e-rsville District, Georgia: American Institute of Mining
Engineers Transactions, v. 30, p. 403-419.
Higgins, M.W., Atkins, R.L., Crawford, T.J., Crawford, R.F.,III, and Cook, R.B., 1984, A brief excursion through two thrust stacks that comprise most of the crystalline terrane of Georgia and Alabama: Georgia Geologic Survey 19th Annual Field Trip Guidebook, 67 p.
Hurst, V.J., and Crawford, T.J., 1970, Sulfide Deposits in the Coosa Valley Area, Georgia: Coosa Valley Area Planning and Development Commission, 190 p.
Jackson, K.C., 1970, Textbook of Lithology: New York, McGraw Hill, 552 p.
29

Kesler, T.L., 1950, Geology and Mineral Deposits of the Cartersville District, Georgia. U.S. Geological Survey Professional Paper 224, 97 p.
King, P.B., 1950, Tectonic Framework of the Southeastern States: American Association of Petroleum Geologists Bulletin, v. 34, n. 4, p. 635-671.
Kramer, C.Y., 1956, Extension of multiple range tests to group means with unequal numbers of replications: Biometrics, September 1956, p. 307-310.
Lovering, T.G., 1962, The origin of jasperoid in limestone: Economic Geology, v. 57, p. 861-889.
Mack, G.H., 1980, Stratigraphy and Depositional Environments of the Chilhowee Group (Cambrian) in Georgia and Alabama: American Journal of Science, v. 280, p. 497-517.
Maynard, T.P., 1912, A report on the limestones and cement materials of North Georgia: Georgia Geologic Survey Bulletin 27, 293 p.
McLemore, W.H., and Hurst, V.J., 1970, The carbonate rocks in the Coosa Valley area, Georgia: Coosa Valley Planning and Economic Development Administration and U.S. Department of Commerce, 170 p.
Munyan, A.C., 1951, Geology and mineral resources of the Dalton Quadrangle, Georgia-Tennessee: Georgia Geologic Survey Bulletin 57' 128 p.
Pierce, W.G., 1944, Cobalt-bearing manganese deposits of Alabama, Georgia and Tennessee: U.S. Geological Survey Bulletin 940-J, p. 271-183.
Pringle, J.S., 1967, Taxonomy of Gentiana, Section pneumonanthae, 1n eastern North America: Brittonia, v. 19, n. 1, p. 1-32.
Rich, J.L., 1934, Mechanics of low-angle overthrust faulting as illustrated by Cumberland Thrust Block, Virginia, Kentucky, and Tennessee: American Association of Petroleum Geologists Bulletin, v. 18, p. 1584-1596.
Salisbury, J.W., 1961, Geology and mineral resources of the northwest quarter of the Cohutta Mountain Quadrangle: Georgia Geologic Survey Bulletin 71, 61 p.
Shearer, H.K., 1918, Report on the Slate Deposits of Georgia: Georgia Geologic Survey Bulletin 34, 192 p.
Smith, J.W., 1959, Geology of an area along the Cartersville fault near Fairmount, Georgia (MS thesis): Atlanta, Emory University, 41 p.
Smith, J.W., Wampler, J.M., and Green, M.A., 1969. Isotopic dating and metamorphic isograds of the crystalline rocks of Georgia, in Precambrian-Paleozoic Appalachian problems: Georgia Geologic Survey Bulletin 80, p. 121-139.
30

Smith, W.L., 1958, The Geology of the Conasauga .Formation in the vicinity of Ranger, Georgia (MS thesis): Atlanta, Emory University, 33 p.
Spalvins, K., 1969, Stratigraphy of the Conasauga Group in the Vicinity of Adairsville, Georgia (MS thesis): Georgia Geologic Survey
Bulletin 80, p. 37-55. Spencer, J.W.W., 1893, The Paleozoic group: the geology of ten counties
of northwestern Georgia: Georgia Geologic Survey Bulletin, 406 p. Stuart, A.W., 1956, A detailed petrographic study of the Paleozoic
sediments in the area of Fairmount, Georgia (MS thesis): Atlanta, Emory University, 33 p. Valentine, J.W., 1978, The evolution of multicellular plants and animals: Scientific American, v. 239, n. 3, p. 141-158. Wegener, A., 1966, The origins of continents and oceans: New York, Reprinted by Dover Publications, 246 p.
31

o4 4o; 7Q]OOOM E.

7()9

4. 22 '30"

40!i2 I NW
!FAIRMOUNT!

PLATE lA

117

360 000

8437'30" 34. 22' 30"

1 590000

(
I
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?

20'
311()!
tne

\



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C"J'"U'.

A'

EXPLANATION

I~

CONASAUGA SH ALE

f] oaj 500 CONASAUGA L IMESTONE

! ! I 500' ROME DOLOSTONE

~ 950 ROME SHALE AND SANDSTONE

[sj 100'+ SHADY DOLOMITE
~ 100 0' CH I LHOW EE GROUP
OCOEE GROUP
......__ F AULT

0L . __

__10L0_ 0 __2j000 FEET

GEOLOGIC MAP OF THE PINE LOG CREEK AREA: FORMATIONS AND CROSS SECTIONS.

311()2

EXPLANATION
~CONA S AUGA LIM ESTONE
Rf~) CONASAUGA SHALE

f-;;"Rsbi ROME SHALE AND S ANDSTON E
lEt;! SHADY DOLOMITE
fiE] CHILHOWE E GfiOUP
t~~J OCOE E GROUP

'f 6

THRUST fAULT (Great Smo ky)

- - - PROBABLE FAUtL.T

1 MILE

_J
!

84"45'70~[.

101

4. 22'30"

42' 30"

loQ!J2 I NW
fFAIRMOUNTJ

PLATE 18

SW/4 WALESKA 15' QUADRANGLE

84"37'30" 34. 22'30"

\

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GEOLOGIC MAP OF THE PINE LOG CREEK AREA: FIELD DATA.

l

EXPLANATION

ANT IC LINE SY NC LIN E

- 4 - MINOR ANTICL INE
~- MINOR SYNCLINE

56 24
a a o

H O R IZ ON T A L BEDD ING S T R IK E AND D IP OF BEDDING STRIKE AND D IP OF CL E AVAG E THRUST FAUL T (Great Smo ky )

MINE OR PRO SPEC T

0

SI NK HOLE

S P R I NG

LIM E ST ON E OR DOLOS T ONE OUTCROP

!lt1

SAN DS TON E OUT CRO P

QUAR T Z IT E OUTCROP



S HA LE OU T CROP

JAS PEROID, OU T C ROP OR FLO A T

0

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31()1

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