Geology and ground-water resources of Floyd and Polk Counties, Georgia

~ INFOCRMIARTIOCNULAR~
GEOLOGY AND GROUND-WATER RESOURCES OF FLOYD AND POLK COUNTIES, GEORGIA
by
Charles W. Cressler
THE GEOLOGICAL SURVEY OF GEORGIA DEPARTMENT OF MINES, MINING AND GEOLOGY
Jesse H. Auvil, Jr. State Geologist and Director
ATLANTA
1970

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GEOLOGY AND GRO UND - WATER RESOURCES OF FLOYD AN D POLK COUNTIES, G EORG IA
by
Charles W. Cressler
THE GEOLOGICAL SURVEY OF GEORGIA DEPARTMENT OF MINES, MINING AND GEOLOGY
PREPARED IN COOPERATION WITH THE U.S. GEOLOGICAL SURVEY ATLANTA 1970

CONTENTS

Abstract . . Introduction
Location and extent of area . Physiography, topography, and climate Purpose, scope, and methods of investigation Well and spring numbering system Previous investigations . Acknowledgments . . Geologic formations and their water-bearing properties Cambrian System .
Shady Dolomite Rome Formation . Conasauga Formation

Cambro-Ordovician Sediments . .

Knox Group

.....

Copper Ridge Dolomite Chepultepec Dolomite . Longview Limestone Ordovician System . .

Newala Limestone Lenoir Limestone

Mosheim Member Deaton Member Rockmart Slate

Other formations of Ordovician age .

Silurian System

Red Mountain Formation

Devonian System . . . .

Frog Mountain Sandstone

Armuchee Chert .

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Page No. 1 1 1 2 2 3 3 3 4 4 4 6 9
13 13 13 13 13 16 16
20 20 22
23 32
34
34
36
36
39

CONTENTS--Continued
Geologic formations and their water-bearing properties--Continued Chattanooga Shale . Maury Member
Mississippian System Fort Payne Chert
Lavender Shale Member Floyd Shale . . . . .
Hartselle Sandstone Member Bangor Limestone Pennsylvanian System . Cambrian to Pennsylvanian Systems Talladega Slate . Geologic structure Indian Mountain Etna Valley . . Utilization of ground water . Water-level fluctuations Summary of ground water References . . .

Page No.
40 40
41 41
45 47 48 50 50
51 51 52 53
54 54 54 55 56

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CONTENTS Illustrations

Figure 1. 2. 3. 4. 5. 6. 7. 8. 9.
10.

Index map of Georgia . Ground water availability map, Floyd County . Ground water availability map, Polk County Map of Floyd County showing geology, wells, and springs Map of Polk County showing geology, wells, and springs Photograph showing conglomerate in Rockmart Slate . Photograph showing conglomerate pebbles . Photograph showing beds of sandstone in Rockmart Photograph of cuts of the Southern Railway Photograph showing inclined Fort Payne Chert

Page No. 1 5 7
in pocket in pocket
24 31 32 33 43

APPENDICES Appendix A
Fossil Illustrations
Plate 1 Characteristic Cambrian and Ordovician fossils Plate 2 Characteristic Ordovician and Mississippian fossils

Page No. 61 63

iii

Appendix B

Tables

Table 1. Geologic formations and their water-bearing properties, Floyd

and Polk Counties, Ga. . . . . . . . . . . . . .

66

2. Chemical analyses of ground water, Floyd and Polk

Counties, Ga. . . . . . . . . . .

68

3. Spring flows in Floyd and Polk Counties, Ga.

69

4. Graptolites from the Rockmart Slate, indicated by localities

72

5. Middle Ordovician graptolite zones of Berry (1960)

73

6. Record of wells in Floyd County, Georgia

74

7. Record of wells in Polk County, Georgia .

86

iv

GEOLOGY AND GROUND-WATER RESOURCES OF FLOYD AND POLK COUNTIES, GEORGIA
by
Charles W. Cressler U. S. Geological Survey

ABSTRACT
Floyd and Polk Counties are mainly in the Valley and Ridge province of Georgia but extend a short way into the Piedmont province. They are underlain by formations ranging in age from Early Cambrian to Pennsylvanian.
Over most of the area, except on ridges and steep slopes, ground water is available from wells in sufficient quantities for domestic and farm supplies and the quality of the water generally is good. Wells yielding 600 to 1,500 gpm (gallons per minute) are found locally, and the water, although hard, is low in iron content and is suitable for many industrial needs.
Good quality spring water that is moderately hard to hard and has a low iron content discharges from several springs in amounts ranging from less than 0.5 mgd (million gallons per day) to nearly 15 mgd.
The Newala Limestone, of Early Ordovician age, is the most productive aquifer in the area. Seven springs that have a combined flow of more than 24 mgd discharge from it; and most of the wells in the area yield water from this formation.
Geologic mapping resulted in several significant changes, among them: The Rockmart Slate was reassigned from Mississippian age to Middle Ordovician; areas formerly mapped as Weisner Quartzite (Cambrian) were found to be underlain by Newala Limestone (Ordovician) and younger formations; and the iron in the important iron mining area of western Polk County was found to be in the residuum of the Newala Limestone rather than of the Shady Dolomite (Cambrian).
INTRODUCTION

culture in northwest Georgia (fig. 1). Among the wide variety of goods produced there are paper, cement, rayon, crushed rock, textiles, electricity, and electrical products. Floyd County, with a population of more than 69,000 (1960 census) ranks 12th in the State, and Polk County with over 28,000 people ranks 29th. Together the counties include 826 square miles.

85"

84"

---.---84" 83" 50
Figure 1. Index map of Georgia showing location of Floyd and Polk Counties.

Location and Extent of Area
Floyd and Polk Counties form one of the most important centers of business, industry, and agri-

Rome, the county seat of Floyd County and the largest city in the report area, is at the confluence of the Etowah, Oostanau1a, and Coosa Rivers. It is

1

connected by U. S. Highway 27 to Chattanooga, Tenn., 70 miles to the north, and to Cedartown, 15 miles to the south. U. S. Highways 411 and 41 give Rome access to Atlanta, some 70 miles away to the southeast.
Cedartown, the county seat of Polk County, is at the intersection of U. S. Highway 278, which connects it to Atlanta and to points west in Alabama, and U. S. Highway 27 which gives ready access to Floyd County on the north and Haralson County to the south.
The Counties are served by the Southern Railway, the Seaboard Coastline Railroad, and the Central of Georgia Railway.
Physiography, Topography, and Climate
Nearly all of Floyd and Polk Counties is in the Valley and Ridge physiographic province; only the southern and eastern edge of Polk County extends into the Piedmont physiographic province. Northwestern Floyd County, the most mountainous part of the study area, has a terrain of narrow valleys whose bottoms are between 600 and 700 feet above sea level, bordered by steep ridges whose tops range from 1,400 to 1,600 feet above sea level. The terrain in the remainder of Floyd County and in most of Polk County consists chiefly of lowlands and hilly areas that range in altitude from about 600 to 1,000 feet. A few isolated ridges occur there but most have altitudes less than 1,300 feet and only one, Indian Mountain in western Polk County, reaches 1,500 feet above sea level.
The part of Polk County lying in the Piedmont province is a moderately dissected plateau having rounded hilltops and narrow stream valleys. The plateau stands about 500 feet above the adjoining lowlands of the Valley and Ridge province and is separated from them by a fault-line scarp. In Polk County the plateau attains a maximum altitude of about 1,300 feet.
Floyd and Polk Counties have a mild climate. Their average January temperature is about 43 F. and their average July temperature is about 800 F. The average annual precipitation in the two counties is about 53 inches and includes only a small amount of snow.

Rainfall in this part of the State has two peaks, one in winter and one in midsummer, separated by periods of lighter rains in spring and autumn. Autumn is the driest season of the year. Large variations can occur in the amount of rainfall received from year to year, and amounts from the wettest years may be about double that for the driest years. Nearly half of the rainfall comes in amounts of 1 inch or more within 24 hours.
Dry spells occasionally cause heavy damage to crops and pastures and result in shortages in water supplies. Droughts of this severity are, however, usually limited to rather small areas so that any given locality, on the average, is not likely to have a serious drought more often than once in 10 to 15 years.
Purpose. Scope and Methods of Investigation
This investigation was made by the U. S. Geological Survey in cooperation with the Georgia Department of Mines, Mining and Geology, as part of a statewide appraisal of ground-water resources. The purpose of the investigation was to determine the amount and chemical quality of water available in Floyd and Polk Counties, and to describe and delineate the aquifers from which it comes. This study covers 2 of 10 counties in the Paleozoic rock area of Georgia; studies of Catoosa, Chattooga, and Walker Counties (Cressler, 1963, 1964) and of Dade and Bartow Counties (Croft, 1963, 1964) have been completed and the results already published.
In making this study, more than 700 wells were inventoried to learn the range in well depth, the depth to water, and the quality and quantity of the water being taken from the various aquifers. Periodic measurements were made on several wells to indicate the amount of seasonal fluctuation that occurs in the water table.
Springs of significant size were inventoried and their rate of flow measured or estimated. The temperature of the spring water was recorded, and the reliability, degree of fluctuation, and the quality of the water were ascertained where possible.
Water samples were taken from 8 wells and 16 springs for chemical analyses by the Quality of Water Laboratory, U. S. Geological Survey, Ocala, Florida.

2

To delineate the various aquifers and determine their lithologic character and their thickness, the geology of the counties was mapped using aerial photographs as a base. Fossils were used, wherever obtainable, to assure accurate age determinations and correlations. Fossil collections were identified by personnel of the Paleontology and Stratigraphy Branch of the U. S. Geological Survey and their identifications and assigned ages are included in this report.
Fossils found during the investigations revealed, unexpectedly, that some formations in the area had been incorrectly dated, that geologic structures had been misinterpreted, and that some formations had previously neither been recognized nor mapped. As solving these problems would require more time than was alloted the project, an extension was arranged to allow for more geologic mapping. Because of the resulting new information and interpretations, the larger part of this report is devoted to geology.
Well and Spring Numbering System
Wells in this report are numbered according to a system based on the 7%-minute topographic quadrangle maps of the U. S. Geological Survey. Each 7%-minute quadrangle in the State has been given a number and a letter designation according to its location. The numbers begin in the southwest corner of the State and increase numerically eastward. The letters begin in the same place, but progress alphabetically to the north, following the rule of "read right up." Because the alphabet contains fewer letters than there are quadrangles, those in the northern part of the State have double letter designations, as in 5HH.
Floyd and Polk Counties are covered by all or part of 23 quadrangles (figs. 4 and 5). Wells in each are numbered consecutively, beginning with number one as in 5HH1. Springs in each quadrangle are numbered similarly except that the letter "S" is added to distinguish them from wells, as in 5HHS1.
Previous Investigations
The general geology of the area was discussed in early reports by Smith (1890), Hayes (1891, 1892, 1894, and 1902) and Spencer (1893). The most recent publication dealing with the general

geology was by Butts and Gildersleeve (1948). Several reports dealing with specific aspects of the geology and mineral resources of the area have been published as bulletins of the Georgia Geological Survey; a list of those available can be obtained from the Georgia Department of Mines, Mining and Geology, 19 Hunter Street, S. W., Atlanta, Georgia 30334. Other detailed work has been done by graduate students of Emory University for Masters theses.
Acknowledgments
The writer expresses his appreciation to the citizens of Floyd and Polk Counties for their cooperation in furnishing information for the well and spring inventory, and for their aid in collecting water samples for chemical analyses.
Acknowledgment is due the many persons who contributed in various ways to the investigation. Drs. Arthur T. Allen and R. J. Martin of the Emory University Geology Department contributed greatly to working out the structure of Turkey Mountain. Mr. Ernest W. Renshaw, geologist with American Cyanamid Company, offered many helpful suggestions, particularly concerning the structure and stratigraphy of the Knox Group, and supplied data about ground-water conditions in the residuum of the Knox. Dr. Robert D. Bentley accompanied the writer in mapping and correlating the Talladega Slate from its type locality in Alabama into Polk County, and was very helpful in interpreting several geologic phenomena. Dr. A. S. Furcron, former Director, Georgia Department of Mines, Mining and Geology, discussed geolgoic problems with the writer and made available unpublished information he had obtained on the area.
The writer is especially indebted to Drs. Robert B. Neuman and Ellis L. Yochelson of the Paleontology and Stratigraphy Branch of the U. S. Geological Survey who came to the study area to collect fossils, and assist in working out the stratigraphy; and to Dr. John Rodgers of Yale University who visited the counties and offered valuable suggestions about the geologic interpretations. Special thanks are due Mr. Thomas J. Crawford who made visits to the Indian Mountain-Etna Valley area to show the writer mines, outcrops, and fossil localities and who generously made available his field notes on the area and the fossils

3

he collected during a study made for a Masters thesis.
Mr. Horace Sheffield and many other students from Shorter College in Rome, and Dr. Lewis Lipps, Professor of Geology at Shorter, collected and cataloged numerous fossils from Polk County. Mr. Allen Sheldon and Dr. Lipps were instrumental in bringing to the writer's attention the excellently preserved Middle Cambrian trilobites obtained from the banks of the Coosa River. Mr. Cyrus Pope was generous enough with his time to spend a day guiding the writer to dozens of iron mines in the rugged terrain around Indian Mountain.
Dr. William B. N. Berry of the University of California, Berkeley, identified the graptolites collected from Polk and Murray Counties, Ga.
Plates of fossils for the report were prepared by the Paleontology and Stratigraphy Branch of the U. S. Geological Survey under the direction of Dr. Ellis L. Yochelson.
This investigation was started under the direct supervision of H. B. Counts, former district engineer, Ground Water Branch, and completed under A. N. Cameron, district chief, Water Resources Division, Georgia District, U.S. Geological Survey.
Mr. Harry E. Blanchard, Hydraulic Engineering Technician, made the complete well inventory of Polk and Floyd Counties and collected water samples for chemical analyses.
GEOLOGIC FORMATIONS AND THEIR WATER-BEARING PROPERTIES
Floyd and Polk Counties are underlain by more than 20 geologic formations that have an aggregate thickness of several thousand feet; they range in age from Early Cambrian to Pennsylvanian. Originally the formations were horizontal, but compressional and tensional forces later warped them and broke them into a series of faulted folds. Erosion of the folded and faulted formations produced the varied outcrop pattern that exists today.
In order to appraise the ground-water resources of an area, it is necessary to know the lithology, thickness, and topographic setting of the geologic formations there. This information for Floyd and Polk Counties is summarized in table 1 and is discussed in more detail in the text that follows. The generalized availability of ground water in the

counties is shown in figures 2 and 3. The detailed outcroppings of the formations and structural cross sections are given on the accompanying geologic maps, figures 4 and 5.
Cambrian System
Shady Dolomite
Along the trace of the Coosa fault between Rome and Cave Spring, the Rome Formation is underlain by a unit of dolomite that tentatively is being correlated with the Shady Dolomite of Early Cambrian age. The Shady, named by Keith (1903, p. 5) for Shady Valley, Johnson County, Tenn., normally occupies a position below the Rome, separating it from the Weisner Quartzite. As the dolomite in Floyd County occupies the same stratigraphic position and is of a similar character, it is being correlated with the Shady.
Lithology and thickness.-In Floyd County, on
the north bank of Big Cedar Creek about 300 feet east of the bridge on Spout Springs Road (fig. 4), the exposed Shady consists of a lower 20-foot unit and an upper 10 to 15-foot unit of thinly to massively bedded, commonly shaiy dolomite, separated by about 10 feet of dark shale and very thin bedded earthy dolomite that weathers to shale. The upper dolomite layer is succeeded by 5 feet of dark-gray shale that passes abruptly upward into maroon shale and siltstone of the Rome Formation.
The dolomite is mainly medium to dark gray, very thickly to massively bedded and fine grained. Much of it contains large amounts of silt and clay that either weathers out as shale or accumulates on the surface as an olive-gray, tan, or yellowishbrown crust. Where the dolomite is deeply leached, the impurities form a tan shale residuum. The residuum is well displayed in the first road cut southeast of the creek bridge.
In natural exposures the Shady is dotted by rounded to irregularly shaped pieces of highly fractured light-gray quartz that protrude from its surface, an occurrence not observed on any other formation. Much of the dolomite is crisscrossed by numerous fractures filled by light-gray quartz. Some outcrops are so highly fractured that about half of the rock consists of quartz fracture fillings. One outstanding feature of the Shady is the complete absence of bedded or nodular chert.

4

E X PL A N A T

0 N

Sandstone and chert
Yield 0 to 10 CJPm on narrow ridCJes ; 0 to 20 CJPm on broad r i does . Water soft, most hioh in iron.
D
Ma i nly shale
Yields 0 to 5 opm on hills; 5 to 20 gpm i n most other areas . Water soft to hard , commonly high in iron; some requires treatment .

lr~~
Chert
Yields 5 to 100 CJPfl'l i n most areas except steep slopes . Water soft, low in iron .
~ ~
Lime stone, siliceous HloMite, ond chert
Yi elds 5 to 20 CJP"' in most area; more than 200 CJP"' l oca l ly. Water hard , low in iron .

N

5

0

5 MILES

1

85 15'

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:... ..:...:. :... :....:..:... :... .:.. :.....:. .:...:..:... :... .:...:..:...:.....:. I

::::: :::: : :: :::::::: .

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-

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Figure 2. Generalized availability of ground water to wells in Floyd County.

The presence of the Shady Dolomite in Polk County has not been established firmly, but two outcrops there have lithologies that are similar to the Shady in Floyd County and therefore are correlated with it. One outcrop, which is about 2 miles south-southeast of Van Wert, is a 30 to 50-foot section of dolomite faulted between the Rockmart Slate and the Cartersville Fault. The dolomite is medium to dark gray, massively bedded, finely crystalline, and somewhat earthy. Some weathered layers have small pieces of light-gray quartz protruding from their surfaces, similar to those on the Shady in Floyd County, but the rock is almost entirely free of chert.Fractures, widely spaced in most of the outcrop but locally abundant, are filled with white quartz. In nearly all respects, this dolomite closely resembles the dolomite of the Shady along Big Cedar Creek in Floyd County.
Dolomite that underlies the valley 1.5 miles southwest of Van Wert was identified as Shady. It is medium to light gray, thickly to massively bedded and finely crystalline and may be as much as 100 feet thick. Although the dolomite is generally chert free, it is earthy and produces a residuum of siltstone or very fine grained quartzite, plus other siliceous material that resembles jasperoid.
Distribution.-A few feet of the Shady is exposed on Park Drive, north of the Floyd County Public Works Camp. A thin section of the formation crops out between the Rome Formation and the plane of the Coosa fault, in a large cleared area on the west side of the ridge about a mile north of Park Drive. The best exposures of the Shady and the ones showing the contact with the Rome Formation occur on the north bank of Big Cedar Creek, east of the bridge on Spout Springs Road, and in the first road cut southeast of that bridge.
The Shady in Polk County crops out beneath the Cartersville fault about 2 miles south-southeast of Van Wert, and in the valley 1.5 miles southwest of Van Wert.
Stratigraphic relations.-As the contact between the Shady and the Rome Formation is gradational, the contact was placed at the base of the lowest bed of maroon shale in the Rome. The dark-gray shale overlying the dolomite of the Shady was included as part of the Shady because similar shale

occurs lower in that formation, whereas nothing like it occurs in the Rome. The contact is well displayed on the north bank of Big Cedar Creek and along the road southeast of the creek bridge.
Hydrology.-The Shady seems to have little potential as an aquifer along most of its outcrop in Floyd County because it underlies steep slopes. Domestic supplies may be obtainable in the few places where the formation is dissected, such as the low area near Park Drive south of Rome. Larger yields may be available where the Shady is crossed by Big Cedar Creek, but the area in which to place a well is small and by having to drill close to the Creek, there is a likelihood of pumping surface water.
The Shady in Polk County is an aquifer only in the valley 1.5 miles southwest of Van Wert where it underlies a broad low area that has recharge available from a stream. Wells there probably will supply from 5 to 50 gpm or more. Well 5FF15, which is 186 feet deep and cased to 80 feet, supplies a home and farm. The well water is hard, but otherwise is of good quality.
A pool spring on the valley floor has a small discharge that is used as a domestic and farm supply.
Rome Formation
The Rome Formation of Early Cambrian age was named by Hayes (1891, p. 143) for exposures south of Rome, Ga. No type section was specified, but Hayes probably named the formation for exposures on the ridge that now is crossed by Park Drive and Walker Mountain Road. The massive quartzites in the upper part of the formation are particularly well displayed on Walker Mountain Road.
Lithology and thickness.-The Rome consists of between 500 and 1,000 feet of interbedded shale, siltstone, sandstone, and quartzite, in that order of abundance. Most of the shale and much of the thin-bedded sandstone and siltstone are brightly colored in hues of red, purple, green, yellow and brown. Alternating layers of varicolored rock produce a striking effect that is unique in the area. Most of the thick layers of sandstone and quartzite are very light gray, but upon exposure alter to tan or rusty brown. Thickly layered sandstone and quartzite occur mainly in the upper half and

6

\:

N
__r----------J 1

0

S IIIJLES

EXPLANATION

Sandstone and chert
Yields 0 to 5 gpm on narrow r idges; somewhat more on brood ri dges Water soft to moderately hard, genera ll y hi gh in iron
D .. . .
Limestone, siliceous dolomite, and chert
Yields 5 to 20 gpm in most areas ; 200 gpm or more locally Water hard, low in iron .

D
Slate and shale
Yields 0 to 5 gpm on hi lls; 5 to 300 gpm i n volleys . Water soft to ha r d, some high in i ron .
D
Phyllite, quartzite, and graywacke
Yields 0 to 10 gpm on hi lls, steep slopes; 5 to 20 gpm i n most other a r eas . Water soft to hard , much high in iron,

Limestone and dolomite Yields 2 to 20 gpm in most areas; 600 to 1500
gpm in some vo II eya . Water hard, low in iron.
Figure 3. Generalized availability of ground water to wells in Polk County.

7

are most abundant near the top of the formation.
A good exposure of the Rome and one that shows the rarely exposed base of the formation can be seen along the bank of Big Cedar Creek, east of the bridge on Spout Springs Road. The lower 50 feet of the Rome consists of red or maroon shale and thin-bedded reddish siltstone. This is followed by 100 or more feet of red and tan siltstone and a little maroon shale containing very fine-grained sandstone in beds 3 to 6 inches thick. The middle part of the Rome is made up chiefly of thin-bedded, generally fine- to medium-grained white, yellow, tan, purple, and pale red sandstone intercalated with similarly colored siltstone and red, purple, green, tan, or yellow shale. The upper one-third of the formation is composed of shale and siltstone almost the same as that lower down, but it is interbedded with sandstone and quartzite that increases in abundance and becomes thicker bedded toward the top. Layers 2 to 4 feet thick are common and a few beds exceed 6 feet in thickness. Where fresh, the sandstone and quartzite are light gray, but upon exposure they change to light brown.
The quartzite in the upper part of the Rome varies somewhat in character with the locality. In the City of Rome, at the intersection of Glenn Milner Boulevard and East 6th Avenue, the quartzite is very fine grained, massive, thougli thinly bedded, and has a banded weathering surface caused by the alternation of light to medium-gray, and tan-weathering layers. The quartzite forming the low ridge between the tracks of the Southern Railway and the Central of Georgia Railway, between the Lindale and Old Lindale Highways just south of Rome, is very fine grained, laminated, and crossbedded. It is composed principally of rounded quartz grains and contains some detrital feldspar grains (Laurence, 1961, p. 39).
The thickly to massively bedded very finegrained quartzite and maroon shale that forms the small ridge above the Shady Dolomite in the valley 1.5 miles southwest of Van Wert, Polk County, tentatively is identified as Rome on the basis of its lithology and the assumption that the underlying rock is correctly identified as Shady.
Northeastward from Rome, the formation becomes progressively less sandy; sandstone beds are fewer, thinner, and finer grained. The upper one-

fourth of the formation, in contrast to the section south of Rome, is almost devoid of sandstone. Much of the upper shale lacks the characteristic bright colors, making it difficult to deternrine accurately the top of the formation. Several layers of material in this part of the outcrop appear to have been derived from carbonate.
Distribution.-The Rome is fairly resistant to erosion and makes up a series of knobby ridges of moderate relief that reach diagonally across Floyd County. From the Alabama State line near Cave Spring, the ridges extend northeastward through Rome and Shannon. Almost all exposures of the Rome are faulted on the west or northwest side, so that only the upper half to three-quarters of the formation crops out. The entire section of the Rome appears at the surface only along segments of the Coosa Fault between Rome and Cave Spring, where the Shady Dolomite replates the Rome Formation as the base of the Coosa thrust sheet.
The formation is well displayed at several places within the city limits of Rome, especially east of the Civic Center and near the Fair Grounds. The Rome was uncovered south of East Rome Elementary School during construction of the south extension of Turner McCall Boulevard. Massively bedded quartzite typical of the upper part of the Rome is exposed beside Glenn Milner Boulevard at East 6th Avenue. Dolomite that may belong to the Rome, but which may be part of the Shady, crops out just north of Glenn Milner Boulevard at East 4th Avenue.
So far as is known, outcrops of the Rome in Polk County are limited to the faulted ridges about 2 miles west of Georgia Highway 101 at the Floyd County line and to the low ridge along the south side of the valley, 1.5 miles southwest of Van Wert.
Stratigraphic relations.-on Walker Mountain Road, the highest sandstone bed in the Rome Formation is overlain by several feet of varicolored shale and siltstone of the typical Rome type. Thus, the uppermost sandstone layer is not a satisfactory indication of the top of the formation as was suggested by Hayes (1902).
The highest colored shale and siltstone of the Rome are followed by several feet of yellow and tan, rather nondescript shale, and very thinly bedded siltstone that grade upward into greenish and

8

tan-weathering shale of the Conasauga Formation. Every place where the contact between the Rome and the Conasauga was observed, it appeared to be gradational, the transition taking place through an ill-defined zone about 10 feet thick.
Hydrology.-Ground water in the Rome occurs mainly in secondary openings produced by fracturing and jointing and, thus, is available primarily from the thicker layers of siltstone, sandstone, and quartzite. Yields from the Rome generally are smaller than from other sandstone aquifers in the area, because the large amount of shale in the formation impedes the downward movement of water, reducing the rate of recharge.
Wells inventoried in the Rome Formation range in depth from about 80 to 140 feet and average about 100 feet deep. In the upper part of the formation where sandstone and quartzite layers are better developed, wells generally yield between 5 and 10 gpm, and some reportedly will furnish 20 gpm. Lower in the section where shale is the predominant rock type, yields are generally around 1 or 2 gpm.
The well water reportedly varies from soft to hard, though most of it is soft and some contains a high concentration of iron. Water sampled from well 5JJ21 had a total hardness of 53 ppm (parts per million) and an iron content of 0.07 ppm (table 2).
Conasauga Formation
The Conasauga Formation of Middle and Late Cambrian age was named by Hayes (1891, p. 143, 144-145) for exposures along the Conasauga River in Whitfield and Murray Counties, Ga.
In the area of this report, the Conasauga occupies two belts in which the formation differs significantly; the belts are several miles apart and occupy different depositional environments. The western belt includes all outcrops of the formation in Floyd County northwest of the Coosa Fault. The other, the eastern belt, takes in all of the Conasauga in Floyd County southeast of the Coosa fault, as well as all of the outcrops in Polk County. Because of their lithologic differences, the two belts are discussed separately.
Eastern belt
The Conasauga forming the eastern belt extends

diagonally across Floyd County from the Gordon County line past Rome to the Alabama State line. Branches off the main belt occur in southeast Floyd County and in Polk County.
Lithology, thickness, and distribution.-In the part of the eastern belt lying between Rome and the Gordon County line, the Conasauga consists of limestone and shale in nearly equal proportions. The lower part of the formation is made up of 100 feet or more of medium-gray, massively bedded limestone. A good outcrop of the limestone occurs beside the road about 1.5 miles north of the center of Shannon. The limestone is followed by several hundred feet of olive and tan shale, which is used extensively for the manufacture of brick at Plainville just across the line in Gordon County.
The middle of the formation includes thick, apparently discontinuous layers of massively bedded, medium-gray, oolitic and nonoolitic limestone that grades into and is interbedded with olive and tan shale.
Southwest of Rome, toward Cave Spring, the proportion of carbonate increases so that shale is important only in the lower part of the formation. As can be seen along Big Cedar Creek, the lower part is mainly olive shale that becomes interbedded with and finally is replaced by coarse oolitic, medium gray and dark gray, thickly to massively bedded limestone farther up. The middle and upper parts of the formation are chiefly mediumto dark-gray, massively bedded limestone with only a small amount of yellow and tan-weathering shale scattered throughout or derived from the decomposed limestone. Near the top, the limestone gives way to light- to dark-gray, fine-grained, locally oolitic dolomite. The dolomite is distinctively different from that in the overlying Knox Group, as it has a smooth, rounded weathered surface and lacks the crisscross depressions that typify the weathered rock in the lower part of the Knox. Moreover, it is entirely lacking in bedded or nodular chert. The dolomite is exposed in the cut of U. S. Highway 411, about 1 mile northeast of the bridge over Big Cedar Creek.
Southwest of Cave Spring, carbonate rocks constitute an even greater part of the Conasauga. Limestone apparently dominates the middle part, and dolomite makes up most of the upper third of the formation. Dolomite crops out at several places

9

along U. S. Highway 411 near the Alabama State line. On fresh exposures the dolomite appears to be fairly pure, but upon weathering it leaves a residue of siliceous oolite and a few layers of fine-grained sandstone.
The upper part of the Conasauga consists of several hundred feet of calcareous olive-gray and tan shale interbedded with thick sections of massively bedded, blue-gray ribboned limestone and some gray dolomite. One shale unit is thick and makes up a prominent ridge that runs subparallel to Georgia Highway 53 near the Gordon County line. Ribboned limestone is well displayed near spring 5JJS51 southwest of Hermitage. The proportion of limestone increases upward until it completely replaces the shale at the top of the formation. The uppermost 200 to 300 feet of limestone and dolomite are equivalent to the Maynardville Limestone of Tennessee, as shown by fossils at the U. S. National Museum. The total thickness of the Conasauga northeast of Rome is about 1,500 feet.
From U. S. Highway 411, the Conasauga extends southward for a distance of about 2 miles into Polk County. Although it is not exposed, the soil and topography indicate that the formation there is chiefly limestone and dolomite.
In southeastern Floyd County, exposures are so limited that the makeup of the Conasauga could not accurately be determined. However, the amount of shale present in the reddish carbonate soil indicates that the lithology probably is similar to that in the area northeast of Rome.
Hydrology.-ln the eastern belt, from the Gordon County line to a short way south of Paris Lake, including the outcrops in southeast Floyd County and the one in north-central Polk County, most wells yield between 2 and 25 gpm. The average depth of the wells is about 120 feet, but some are deeper than 300 feet. It may be possible to obtain far higher yields from wells drilled in limestone, as one well in the formation south of Calhoun in Gordon County produced nearly 300 gpm.
The range in well yields largely reflects the different lithologies in the formation. Nearly all of the low yielding wells are in shale, whereas the better producing ones are partly or wholly in limestone. To some extent in the shale, but more

so in the limestone, the amount of water obtained depends largely on the topographic position of the well site; wells positioned near the bottom of local drainage courses normally are the best producers. Even poorly defined drainage courses that flow only during wet periods are good drilling sites, as they tend to concentrate the flow of ground water and increase the quantity available to a well.
The quality of the well water varies from soft to hard, depending on the type of rock from which it is derived. The water generally has a low iron content.
A few springs discharge from this part of the Conasauga but they are small. Spring 5JJS1, about 1.75 miles south of the center of Shannon, flows about 0.58 mgd (million gallons per day) and is used for domestic supply (table 3). Hermitage Spring (5JJS4) has about the same flow. Spring 4HHS3 at Lindale discharges from limestone in the upper part of the formation and is used by an industry. Wells at this site were reported to furnish from 5 to more than 50 gpm; nearly all of the wells supply more than 10 gpm. The wells average about 80 feet deep. The deepest well was 105 feet. Water from this segment of the formation generally is moderately hard to hard.
Along the faulted valley that extends from near Hematite Crossing, Polk County, northward to the Floyd County line, several springs discharging into Little Cedar Creek have a combined flow of 3 to 7 mgd, depending on the time of year. Unfortunately, most of these are seep springs located ~m the poorly drained valley floor and are subject to flooding. Protecting them from pollution would require extensive improvements. Those few that are situated some distance from the creek offer the best possibility for development.
Western belt
The Conasauga, in the western belt, underlies most of the Coosa Valley southwest of Rome and large areas of Floyd County northeast of Rome. The rocks in the belt can be divided into three fairly distinct units although the contacts between them tend to be gradational and faulting and folding has brought about a mixing of types in some areas. Accurate differentiation of the units along much of their length is difficult or impossible because the ground is covered by thick alluvial and

10

...

colluvial deposits. These deposits likewise are a major obstacle to further subdivision of the formation.
Lower Unit
Lithology and distribution.-The lower unit of the western belt crops out in a strip about a mile wide that lies along the southeast side of the Coosa Valley, paralleling the Coosa Fault. It is composed of compact olive-green silty shale and greenish fine to medium-grained sandstone in beds less than 6 inches thick. Both the shale and sandstone are calcareous where fresh. The shale weathers to tan or pinkish orange and in so doing, breaks down into small pieces having irregular surfaces. The lack of planar surfaces on the weathered shale sets it apart from the shale in the remainder of the formation. The sandstone, which is interbedded randomly throughout the shale, weathers to rusty brown. In the area west of Cave Spring, thinbedded limestone occurs with the sandstone and shale.
Close to the Coosa Fault, deformation in the lower unit has been so intense that the shale is crumpled, crenulated, and sheared, and some is reduced to a mass of closely spaced slickensided surfaces. Much of the sandstone is reduced to highly fractured lenses and discontinuous layers 1 to 4 inches thick, crisscrossed by white quartz or calcite fracture fillings.
The lower unit is readily distinguishable from the remainder of the formation by the extremely crumpled and sheared character of its shale, the presence of fractured sandstone, and the angularity of the weathered shale pieces. Moreover, it forms noticeably more rugged and somewhat higher terrain.
Hydrology.-Dnly one well was inventoried in the lower unit. It was 175 feet deep and supplied 8 gpm. Wells in the unit probably can be expected to furnish between 2 and 10 gpm in most areas, and the yield may be appreciably higher wherever sandstone is prominent. The water probably will be soft to moderately hard and may contain significant quantities of iron.
Middle Unit
Lithology and distribution. -The middle unit of the western belt crops out in a band about a mile

wide that parallels the lower unit. Its chief constituent is massively bedded medium to dark-gray limestone, which is interlayered with varying thicknesses of olive-gray and tan shale. Some of the limestone is moderately pure and produces a deep red soil, but most contains a large amount of silt and clay that remains as a tan shale residuum. Except where erosion is active, the residual shale obscures the limestone creating the illusion that shale is the principal constituent of the unit.
A common type of limestone in the unit is made up of half an inch to 2-inch thick layers of relatively pure calcium carbonate that alternate with silty, argillaceous, generally dolomitic layers of about the same thickness. As the rock weathers, the impure carbonate becomes tan or brown in contrast with the gray color of the purer layers to produce a distinctive banded or ribboned surface.
Still other limestone in the unit is very massive, but contains dark gray to black clay and silt laminations about 1 millimeter thick between the beds. The laminations appear as dark, irregular lines on the rock surface. As the limestone is leached, it loosens along the laminations and breaks up into thin slabs. Where the rock has come under severe stress, as in the quarry of the Floyd County Public Work Camp, movement was concentrated along the laminations which became phyllitized and heavily slickensided.
The limestone in the unit, as in nearly all of the Conasauga in the State, has been highly fractured and these openings are filled with white or, rarely, pink calcite and by white quartz.
Hydrology.-Eighteen wells inventoried in the middle unit of the western belt ranged in depth from 68 feet to about 300 feet, averaging about 133 feet deep. Most wells were reported t~ supply between 5 and 10 gpm though most probably are capable of far higher yields. The water is of good quality for domestic use and moderately hard to hard.
Upper Unit
Lithology and distribution.-The upper unit of the western belt occupies a far broader belt than the two lower units combined and probably is much thicker.

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The lower part of the upper unit, having an outcrop width of about a mile to a mile and a half in the Coosa Valley, and one considerably wider northeast of Rome, is mainly olive and tan shale containing a large quantity of thin-bedded limestone and calcareous siltstone. This lithology is well displayed along the two roads between Fosters Mill and the mouth of Big Cedar Creek. It also is exposed in the tongue of the formation that extends along the northwest side of Horseleg Mountain and in the northwest part of Rome.
Just above the lower part of the upper unit is a zone about 3 miles wide having a dominant lithology of dark olive-gray, somewhat silty, shale containing abundant mica flakes. The shale weathers to light olive gray and greenish tan. Distributed throughout the silty shale are zones of very dark gray, fairly pure clay shale, that on exposure alters to tan or very light green. This shale has a high carbon content and is very fossiliferous. Both types of shale contain chertlike siliceous nodules up to about 8 inches across that collect on the ground surface, resembling stream gravel. The nodules long have been of interest to paleontologists and collectors because they commonly have trilobites and other Middle Cambrian fauna preserved on their surfaces.
One layer of this dark-gray clay shale cropping out on the east bank of the Coosa River, about 2 miles northeast of the mouth of Big Cedar Creek, contains a profusion of exceedingly well preserved Middle Cambrian trilobites, virtually all one species, Elrathia georgiensis Resser (see plate 1, fig. 1). This collecting locality, reported by Allen Sheldon, a former student at Cave Spring High School, represents an outstanding assemblage of specimens of various sizes, ranging from less than 0.1 inch to more than 3 inches long.
From about a mile and a half northwest of the mouth of Big Cedar Creek, northwestward to within about a mile of Early, the upper unit is dominated by olive-green and olive-gray silty shale that contains discontinuous l-inch to 4-inch thick layers of brown-weathering siltstone and finegrained sandstone, mainly in the lower part, and very thin nodules and discontinuous layers of impure limestone in the upper part. In the vicinity of Early, however, and along the sm:tth edge of Heath Mountain, the shale contains many beds of

thin- to medium-bedded olive-gray siltstone and medium dark-gray impure limestone, commonly in aggregates more than 100 feet thick.
North of Early and beside Georgia Highway 20 west of Heath Mountain the unit is mainly massively layered, ribboned limestone and tan-weathering shale resembling the uppermost part of the Conasauga in the eastern belt between Rome and Shannon. Owing to a lack of outcrops the character of the unit could not be determined either in the tongue north of Heath Mountain or for any appreciable distance north of Georgia Highway 20, but the type of soil indicates that it is predominately limestone or dolomite.
Hydrology.-Wells in the predominately shale upper unit yield between 3 and 10 gpm. Of 20 privately owned wells canvassed, the average depth was 100 feet; the greatest depth was 225 feet. Water from the shale generally is soft and low in iron content.
In part of the unit containing limestone and calcareous siltstone, wells can be expected to supply from 5 to 20 gpm. The water is moderately hard to hard.
Attempts to develop large industrial groundwater supplies in the upper unit have, in the main, ended in frustration. Of three wells drilled at Georgia Power Company's Plant Hammond, only one was considered successful. The well (3JJ33) was drilled 411 feet through shale and several strata of limestone and supplies about 100 gpm. The water has a dissolved solids content of 119 ppm and an iron content of 0.36 ppm. Another deep well not far to the east penetrated only shale and was essentially dry. A third well to the west penetrated shale and can furnish about 60 gpm; however, as the water has a high hydrogen sulfide content, it is little used.
Several wells were drilled at the Georgia Kraft Company plant in an attempt to develop a water supply, but none was satisfactory. The wells, apparently in shale, would supply only a few gallons per minute and the water contained too much hydrogen sulfide and iron to be used.
A few small springs discharge from the upper unit and are used for watering stock. A sample of water from 3JJS2 had a total hardness of 80 ppm and an iron content of 0.07 ppm.

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Faunal age.-In the western belt, unlike the belt to the east, the oldest part of the Conasauga occurs along the southeast edge of the outcrop. The formation has an overall dip to the northwest and probably is the northwest limb of a broad anticline that was dissected longitudinally by the Coosa Fault. The trilobites Glossopleura sp. and Kootenia sp., collected by Preston E. Cloud, Jr., (1967) from the sandstone-bearing shale along the south edge of the Coosa Valley in Cherokee County, Ala. (on strike with the lower unit of this report), show that part of the formation is Middle Cambrian. Shale in the center of the Coosa Valley in Floyd County contains the trilobite Elrathia georgiensis Resser, and other late Middle Cambrian fauna. Several trilobites from the northern edge of the outcrop at Cedar Bluff, Ala. (Butts, 1926, p. 75), and the trilobites Tricrepicephalus sp. and Acmarhachis ulrichi (Resser) (see plate 1, figs. 2 and 4) from West Rome are of Late Cambrian age (U.S.G.S. CoHn. No. 4415-CO).
Cambro-Ordovician Sediments Knox Group
The Knox Group of Late Cambrian and Early Ordovician age was named by Safford (1869) for developments in Knox County, Tenn. In Georgia, the Knox Group includes three formations: the Copper Ridge Dolomite of Late Cambrian age, followed by the Chepultepec Dolomite and by the Longview Limestone, both of Early Ordovician age (Butts and Gildersleeve, 1948, p. 16).
Copper Ridge Dolomite
Lithology and thickness.-The Copper Ridge Dolomite consists of light- to medium-gray, fine- to coarse-grained, thickly to massively bedded cherty dolomite, and brownish-gray, medium to coarsegrained, asphaltic dolomite that has a distinctive fetid odor on fresh breaks. The brownish-gray dolomite appears to be dominant in the lower part of the formation, but is subordinate to the light gray dolomite in the upper part.
The thickness of the Copper Ridge could not be determined in either Floyd or Polk Counties due to poor exposure, but in Catoosa County, Ga., the only place in the State where the Knox Group has been measured, it is nearly 3,000 feet thick. It may be that thick in western Floyd County and in Polk County.

The dolomite of the Copper Ridge is highly siliceous and yields large volumes of chert and clay residuum. The chert occurs both as layers and as boulder-like chunks that vary from light to dark gray, depending on the state of weathering, and it generally is very hard and vitreous and has a jagged surface. Accumulations of chert and clay create a residual mantle over the formation that generally is between 50 and 200 feet thick and commonly exceeds 300 feet in thickness.
Chepultepec Dolomite
Lithology and thickness.-The Chepultepec Dolomite in the study area has such limited bedrock exposure that its lithology could not be determined. The nearest exposure of the formation is in Catoosa County, Ga., about 50 miles to the north but its lithology probably is similar in both places. In Catoosa County the Chepultepec is about 500 feet thick and consists mainly of light- to mediumgray dolomite in thick to massive layers. Interbedded with the dolomite are a few beds of gray and tan aphanitic limestone. Sandstone occurs near the base and close to the middle of the formation.
The Chepultepec is covered by moderately thick accumulations of chert and clay residuum. Much of the chert is soft and cavernous and, in general, the terrain over the Chepultepec is littered with smaller size pieces of chert that weather from the formations above and below. A few pieces of sandstone may be present in the soil, particularly over the lower part of the formation.
Longview Limestone
Lithology and thickness.-Limited exposures indicate that in Polk and Flqyd Counties the Longview Limestone consists of massively bedded medium- to light-gray dolomite, interbedded with medium- to light-gray aphanitic to medium-grained thickly bedded limestone. In Catoosa County, Ga., the upper part of the formation is roughly 50 percent limestone, but in Polk County nearly all of the formation seems to be dolomite.
The residuum of the Longview tends to be very thick and is littered with large chunks and pieces of hard angular chert and a little sandstone. In Polk County some outcrops of the Longview display chert layers more than 6 feet thick; these break down and show up in the residuum as boul-

13

der-lik_e chunks of chert that litter the landscape.
Fauna and correlation.-The highest outcrops of dolomite and chert on Horseleg Mountain yielded several specimens of Scaevogyra sp. (U.S.G.S. Colin. No. 4417-CO) that are conspecific with material identified by Ulrich and by Butts (1926, p. 88) as Scaevogyra cf. S. swezeyi Whitfield (see plate 1, fig. 3). The species was described from the St. Lawrence Member of the Trempealeau Formation of the Upper Mississippi Valley.
Scaevogyra swezeyi is an excellent guide to the Trempealeauan stage of the Upper Cambrian. According to Ellis L. Y ochelson, it probably is limited to the lower third of the Trempealeau Formation and its equivalents and the fossils from Horseleg Mountain come from a relatively narrow zone, probably just above the middle of the Knox Group.
These fossils show that on Horseleg Mountain the Longview Limestone, the Chepultepec Dolomite, and probably the upper part of the Copper Ridge Dolomite were eroded prior to deposition of the formations of Middle Ordovician age. Great thicknesses of the Knox Group also may have been eroded from other areas west and north of the Rome fault as is suggested by the extreme narrowness of the outcrops there, and by the presence of the Attalla Conglomerate which everywhere marks this unconformity.
Distribution.-The Knox Group has two principal outcrop areas: one lies northwest of the Rome Fault and is confined to Floyd County; the other is southeast of the Coosa Fault and includes nearly all of southeastern Floyd County and a large part of Polk County. Because of the thick mantle of residuum which nearly everywhere covers the Knox, exposures of bedrock are comparatively rare.
Northwest of the Rome Fault the only known exposure of bedrock is on the southwest end of Horseleg Mountain. High up on the mountain the upper part of the Copper Ridge Dolomite is fairly well exposed.
The Knox southeast of the Coosa Fault is somewhat better exposed, but the total thickness cropping out is small. Thin sections of dolomite are exposed at several places along the banks of the Etowah River and in the cuts of U.S. Highway 411

near that river. A few feet of the basal Knox wa~ uncovered beside the paved road that ascends th ridge 1.4 miles southwest of Hermitage. Sandston of the Knox is exposed in several road cuts south and southeast of Wax Lake. Massively bedded chert and a little gray dolomite of the upper part of the Knox crop out on the crest of the ridge, 1.5 miles west of the center of the Rockmart.
All three formations of the Knox Group are present southeast of the Coosa Fault. Massive cryptozoan-bearing chert in the residuum adjacent to the Conasauga Formation shows that the Copper Ridge Dolomite underlies much of southern and eastern Floyd County and large parts of Polk County. Chert carrying the gastropod Lecanospira sp. confirms that the Longview Limestone occupies the expanses of Polk County and southeasternmost Floyd County adjacent to the Newala Limestone. The Chepultepec, evidenced by an unusual amount of soft, cavernous chert and by sandstone beds, underlies the area between. Although these three formations were recognized, no attempt was made to differentiate them because it would have required too much time, and because the three are similar enough lithologically to be treated as a single aquifer.
Hydrology.-More than half of the wells inventoried in the Knox Group are cased to bedrock and derive water from limestone and dolomite; the remaining wells obtain water solely from the residual mantle above the bedrock. As the hydrologic properties of the bedrock and the residuum differ, and because well construction differs in each, the water-bearing character of the bedrock and the residuum are treated separately.
Bedrock wells: Wells penetrating bedrock normally produce large quantities of good quality water. Approximately two-thirds of the wells inventoried yielded between 5 and 80 gpm and all but one well supplied at least 1 gpm.' In depth, the wells average 160 feet; the shallowest well was 50 feet deep, the deepest, 500 feet. Nearly without exception, these wells are cased only a short way into bedrock, leaving the remainder an open hole in rock.
Bedrock wells are most common where the overburden is less than 150 feet thick so that the cost of drilling is not prohibitive. They also are used wherever the desired yield, generally more than

14

10 gpm, cannot be obtained from the residuum or where a high degree of dependability is desired, as they are not appreciably affected by droughts.
Drilling in other areas of northwest Georgia has shown that wells in the bedrock of the Knox will yield from 200 to 300 gpm or more if they are properly located with respect to the drainage. Many of the large watercourses draining the ridges of the Knox are dry much of the year, because water moving along them is beneath the surface. By drilling far enough down a drainage course to insure adequate catchment area above, or better still, by locating a well where a drainage course empties onto a valley or the flood plain of a stream, it is possible to intercept a large volume of ground water.
The quality of water from the bedrock varies from moderately hard to hard and normally has a low iron content. Only a few wells were reported to yield water containing noticeable quantities of iron. Water from well 3FF15 had a total hardness of 160 ppm and an iron content of 0.10 ppm.

able layers is very tight is demonstrated by the fact that test holes placed only 2 to 5 feet apart (unless they penetrate a permeable layer) rarely lose drilling water from one to another even though the water is under a pressure of 100 to 400 pounds per square inch. Thus, it is apparent that appreciable quantities of ground water are available in the residuum only where permeable layers are present.
In developing a well in residuum, it is common practice to drill until a water-bearing zone is reached. If the yield is adequate, casing is set to total depth, leaving only an open hole in the bottom of the pipe to admit water. Thus, because of the restricted intake area, the full potential of the water-bearing zone rarely is utilized. If a well penetrates a thick layer of water-bearing material, or if more than one layer is encountered, slotted casing may be used to increase the yield, but the practice is not common. A few gravel-packed wells have been developed in the residuum, and their yield commonly exceeds 10 gpm.

Wells in residuum: The residual mantle blanketing the Knox Group nearly everywhere is at least 25 feet thick and in many places is more than 300 feet thick. Over most of the outcrop area it probably ranges between 50 and 150 feet thick.
On slopes where it has undergone soil creep, or in low places into which it has been transported, the mantle is a heterogeneous mass of cherty clay having low permeability; wells in this material generally yield 1 or 2 gpm. The remainder of the mantle, however, although it consists mainly of clay, contains well-defined permeable layers.
The only information available about the character of the residual mantle at depth was supplied by Mr. E. W. Renshaw, geologist with American Cyanamid Company, who has directed extensive test drilling in the Knox Group. According to Mr. Renshaw (oral communication, 1966), the mantle which is mainly clay contains layers of silt, sand, sandstone, broken chert, the latter probably derived from the breakup of thick chert beds. These layers appear to have wide lateral extent and, in general, they are very porous and permeable; those that are water-bearing can yield 5, 10, or perhaps as much as 15 gpm to a well.
That the clay material separating these perme-

Rapid declines in yield have been a problem in a few wells cased with solid pipe to total depth. The trouble apparently results from chert fragments, sand, and clay being sucked into the casing. As this material accumulates, the yield declines.
More serious plugging has resulted in some wells that end near the top or near the bottom of a water-bearing zone. Water entering the casing carries loose material with it, leaving a void into which clay may be squeezed by the weight of the overlying material. If clay is forced into the casing, productivity of the well is reduced or stopped. Well 4HH2 went dry after soft material, probably clay, pushed up from below, plugging the casing.
Many people prefer water from the residuum because the water is softer and contains less iron, but well yields generally are less than from the bedrock.
Springs: Several important springs discharge from the Knox Group. In Polk County, Youngs Spring (4FFS3) flows at the rate of about 0.5 mgd. A sample of the water had a total hardness of 108 ppm and an iron content of 0.02 ppm. This is a pool spring situated on the valley floor and would require moderate improvement to prevent pollution. It is only a few yards from the Central of

15

Georgia Railway.
In Floyd County, four principal springs have a combined flow of about 9.5 mgd. The largest flow is about 5.0 mgd from Old Mill Spring (3GGS3), just southwest of the town of Cave Spring. A sample of the water had a total hardness of 96 ppm and an iron content of 0.01 ppm. This is a seep spring that discharges from a wide area so that a considerable enclosure would be required to prevent pollution. The spring is on the side of a ridge, high enough for the water to flow by gravity to the nearby valley. It is about a third of a mile from the Southern Railway.
Cave Spring, in the town of the same name, discharges about 2.5 mgd, half of which currently is being utilized. A sample of this water had a total hardness of 111 ppm and an iron content of 0.03 ppm. As the name implies, this spring flows from a cave so that the water can be obtained before it reaches the surface and no sanitary improvements are required.
Morrison Camp Ground Spring (5JJS2), about 5 miles east of Rome, flows at the rate of about 0.85 mgd. A sample of the water had a total hardness of 54 ppm and an iron content of 0.05 ppm. The spring presently is used for domestic supply and to furnish a summer camp, but only a minor part of the volume is required.
Youngs Mill Spring (5JJS3), about 8 miles east of Rome, is a large seep spring that flows at the rate of about 2.0 mgd. The spring discharges over an area of perhaps an acre, and at present is covered by back water from a private lake. For this reason, a water sample was not taken but the quality should be the same as that of other springs in the Knox. Because this spring discharges in the bed of a wet weather stream and covers a broad area, extensive development would be required.
Spring 5HHS1, about half a mile southeast of Wax Lake, is a seep spring flowing around 1 mgd. Water from the spring had a total hardness of 78 ppm and an iron content of 0.11 ppm. Water seeps from a large area, though it is concentrated in several spring runs. The usefulness of the water will depend on the amount of improvement that is given the spring. Heavy rainfall currently produces a high turbidity, largely from material carried in by surface-water runoff.

Harry Marion Spring (4HHS1 ), about 3 miles southwest of Lindale, discharges 1.2 mgd. The spring water had a total hardness of 116 ppm and an iron content of 0.09 ppm. Because this is a seep spring covering a broad area, it probably would be difficult to develop.
Several other springs discharge from the Knox, but the flow of most is less than 0.5 mgd. A few of the springs presently are being used for industrial or other purposes.
Ordovician System
Newala Limestone
The Newala Limestone of Early Ordovician age was named by Butts (1926, p. 95) for Newala Post Office, Shelby County, Ala.
Lithology.-Dn the east side of Polk County and in southeastern Floyd County, the Newala consists of limestone and dolomite, apparently in nearly equal proportions, although limestone seems to be somewhat more abundant in the upper part. Around Grady and Cedartown, limestone accounts for a larger part of the formation, but dolomite remains prominent.
The limestone varies from light gray to medium dark gray and is fairly pure. Bedding generally is thick to massive, commonly between 1 and 4 feet thick but beds less than 1 foot thick occur. Some beds contain thin sandy zones that weather out in slight relief producing a banded surface. The dolomite is light to medium gray, fine to coarsely grained and most is massively bedded. Some dolomite layers exceed 6 feet in thickness.
The top of the Newala locally is marked by an edgewise conglomerate consisting of argillaceous limestone pieces incorporated in a bed of fairly pure limestone. This conglomerate can be seen in the small quarry 1 mile northeast of the Marquette Cement Company plant near Rockmart, immediately beneath the Lenoir Limestone.
Where the Newala crops out near the Cartersville Fault, the limestone layers are marbleized, but the dolomite remains unaltered. Marbleized limestone interbedded with dolomite is exposed on a low hill south of U. S. Highway 278 (just south of well number 5FF1 7 ), 2 miles southeast of Van Wert. Similar outcrops occur on a hill about 2 miles south-southeast of Van Wert.

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Near Rockmart and Grady and to some extent around Cedartown, the limestone of the Newala has a distinct, though in many places faint, cleavage. The growth of mica along the cleavage planes imparts a foliation to some of the rock that gives the weathered surfaces a slaty look. Where cleavage is strongly developed, the mica layers are very hard and remain in the soil, faintly resembling weathered Rockmart Slate
The cleavage in the limestone generally is subparallel to the bedding, but locally the two planes diverge rather sharply and where the growth of mica is great, the cleavage can be mistaken for bedding. Dolomite beds, however, which are not visibly cleaved are present nearly everywhere and ind~cate the true bedding.
Generally, the Newala contains either widely scattered chert nodules or a few thin discontinuous chert beds, but in a few places it is unusually siliceous and yields both nodular and bedded chert in abundance. Where this occurs at the base of the formation, chert from the Newala gets mixed with chert from the underlying Knox Group, making separation of the two very difficult. The basal part of the Newala is cherty southwest of Cedartown.
Except for the outcrop in the southeast corner, the Newala was not positively identified in Floyd County but the rocks cropping out at the west base of Simms Mountain, a few hundred feet south of the Chattooga County line, may belong to the Newala. At that place, the formations of Middle Ordovician age are underlain by 20 or 30 feet of massively bedded dolomite that is mottled in shades of pink and green and is virtually identical to dolomite in the Newala several miles to the northwest. However, as no fossils were found the identification is questionable, so the dolomite was mapped as part of the Knox Group.
Distribution.-The Newala is present in large areas of Polk County where it underlies valley areas between ridges formed by the Knox Group and the Rockmart Slate. It is widespread in the lowlands around Rockmart, Grady, and Cedartown, and forms a narrow valley extending from Cedartown to Esom Hill. The Newala also forms a large part of the valley at Etna and Oremont.
The Newala is well exposed in the large abandoned quarry at Portland (Davitte), at several

places along the road between Aragon and Taylorsville, and beside the road that runs north out of Aragon. The upper part of the formation is displayed in the quarry about 2 miles north-northeast of the center of Rockmart, and along the south edge of the large quarry beside Georgia Highway 101, immediately north of Rockmart. The Newala crops out on several hills in and near Rockmart and along Georgia Highway 113 between Rockmart and Taylorsville. An excellent exposure of the upper part of the Newala can be seen in the Deaton iron mine west of Taylorsville.
In central Polk County, exposures of the formation are very limited. The upper limestone and dolomite crop out near Antioch School about 3 miles south of Grady and along a creek 1.25 miles southwest of Antioch School, and in a wooded area across the unpaved road half a mile southeast of the latter exposure.
In and around Cedartown, small thicknesses of the formation are exposed in numerous places, particularly along the stream courses. Farther west, it is exposed in the bottom of an abandoned mine 1 mile southwest of Old Brewster School and in the cut of U. S. Highway 278, about half a mile northwest of that school. A few feet of limestone and dolomite of the upper part of the Newala have been exposed in the bottom of an abandoned iron mine on the side of the ridge, about a quarter of a mile southeast of Oremont.
Thickness.-The thickness of the Newala in Polk and Floyd Counties never has been accurately determined, primarily because the formation is overlain by deep colluvium and only partial sections are exposed. Furthermore, the lack of good stratigraphic control precludes piecing together an entire section. Judging by the hills north of Aragon, however, where at least 100 feet of section crop out, and by the great distance to the contact with the Knox Group, it seems probable that the Newala is at least 300 feet thick.
Fauna and correlation.-A key feature of the Newala is its fossils. Calcareous fossils of various types are visible in cross section on the weathered surfaces of much of the limestone, but they are of little use in correlation. Silicified gastropod shells, for the most part poorly preserved, can be collected from the soil in some areas and are helpful in dating. The best guide to the Newala is Cera-

17

topea, a genus whose stratigraphic interval in Georgia is limited entirely to that formation.
The gastropod Ceratopea is best known from its operculum. The ceratopean shell rarely is silicified and therefore is not preserved. The opercula, on the other hand, commonly are silicified and occur with fair abundance in the limestone. They are very resistant to weathering and remain well preserved in the residuum of the formation. Ceratopea is especially important because several species have wide geographic distribution yet are restricted to narrow stratigraphic zones. Thus, the opercula are very useful in interregional correlation.
In Polk County, Ceratopea opercula were used to separate the Newala and the Knox Group where the two formations are lithologically similar. They also were used in conjunction. with other fossils to determine the upper limit of the Newala and establish the contact with the Middle Ordovician Lenoir Limestone. More importantly though, Ceratopea provided the indisputable evidence that enabled a complete reinterpretation of the stratigraphy and structure of the important iron mining center at Etna and Oremont. These fossils make it clear that the iron there is concentrated in the residuum of the Newala Limestone rather than in that of the Shady Dolomite, as previously thought.
Ceratopea opercula have been examined and collected from the Newala in all principal outcrop areas in Polk County, but by far the largest collection and the one containing the greatest number and variety of species came from the residuum in the iron mines near Oremont. More than 300 specimens were taken from a single mine located on the side of the ridge about a quarter of a mile southeast of Oremont (U.S.G.S. CoHn. No. 6294-CO). According to Ellis L. Yochelson this collection includes (see plate 1):
Ceratopea capuli{ormis Oder C. corniformis Oder C. germana Yochelson and Bridge C. incurvata Yochelson and Bridge C. keithi Ulrich C. subconica Oder C. "subconica" Oder C. sulcata Oder C. tennesseensis Oder C. new species?

Other fossils taken from limestone in the bottom of the same mine (U.S.G.S. CoHn. No. 6294CO) include: Orispira sp., indeterminate but probably similar to 0. depressia Cullison; "Helicotoma" unangulata Hall; high spired gastropod aff. "Turritoma ";moderately high-spired gastropod with narrow selenoizone aff. Plethospira; and small operculum. Of this group, Yochelson states, "these fossils all are characteristic of the Newala."
Occurring with the Ceratopea in the uppermost extremity of the mine were specimens of Orospira, Helicotoma, ? Lesueurilla, and the columella of moderately high-spired gastropods. According to Yochelson, the presence of Helicotoma suggests that the Newala in this mine may be overlain by limestone of Middle Ordovician age as it is farther east.
Ceratopea was collected from several other mines in the valley between Etna and Oremont and north of Oremont. They make it clear that the iron ore is concentrated chiefly in the residuum of the Newala Limestone but Lecanospira sp., found in a few mines, indicates that some of the ore probably is in the residuum of the Longview Limestone as well.
Detailed zonations have been worked out for several species of Ceratopea in other parts of the United States (Yochelson and Bridge, 1957, p. 183). From this work, it is known that all of the species found in the Oremont area are from what is roughly the lower half of the Ceratopea zone of other regions. The assemblage from Oremont includes Ceratopea capuliformis Oder which is one of the oldest species known, and C. tennesseensis Oder (see plate 1, figs. 5 and 9), which occurs at about the middle of the zone in the Arbuckle Mountains, in west Texas, and in eastern Tennessee.
The presence of Ceratopea capuliformis Oder on a few mine dumps around Oremont shows that weathering has reached the lowest beds in the Newala in several places, but it does not seem to have progressed to that depth over the whole area. In the mine a quarter of a mile southeast of Oremont, C. capuliformis Oder was brought up from the bottom of a deep funnel shaped ore body that is enclosed in younger limestone. Weathering may extend to the basal part of the Newala only where the downward movement of ground water is con-

18

centrated.
Field studies made by Yochelson and Cressler in 1966 indicate that the highest Newala on the east side of Polk County is in the zone of Ceratopea tennesseensis Oder, the same as the youngest known Newala on the west side of the county. Thus, the fossils so far found show that the Newala across the breadth of Polk County is about the same age, and equals approximately the upper part of the Kingsport Formation and the lower part of the Mascot Dolomite in east Tennessee and equivalents in other regions.
It is not known whether beds of Newala Limestone younger than those now present were deposited in Polk County and subsequently eroded, but this seems likely. Ceratopea unguis Yochelson and Bridge (plate 1) collected in Bartow County, Ga., about 10 miles to the east, is the youngest species of Cera to pea known and shows the Newala there is highest reported in this region. The occurrence of uppermost Newala so close to Polk County indicates that the upper part of the Newala probably was deposited in Polk County, but was eroded prior to deposition of the Rockmart Slate.
Utilization.-Limestone in the Newala of eastern Polk County for many years was quarried to use in the manufacture of cement. The formation, however, never has been a particularly satisfactory source of cement quality limestone because at every location suitable for a quarry at least some dolomite is interbedded with the limestone and must be separated. Several methods of separation were tried including removal of the dolomite by hand but these operations no longer are economically feasible. The more successful quarries were located near the top of the formation where most of the rock is limestone and where a large portion of the recovered rock was the high calcium carbonate Lenoir Limestone.
Hydrology.-The Newala Limestone is the most productive aquifer in the study area. Seven springs discharging from the formation have a combined flow of more than 24 mgd; the largest spring discharges as much as 15 mgd. Wells in the Newala have larger average yields than those in any other formation.
Sixty-seven inventoried wells have an average depth of 147 feet. The shallowest well was 32 feet

deep; the deepest,444 feet. Ninety percent of the wells yield more than 5 gpm, 60 percent furnish more than 10 gpm, and 18 percent supply more than 20 gpm. One well, 4FF21, flows. The highest sustained yield is from well 4GG65 near Cedartown, which is pumped continuously at the rate of 650 gpm; well 3GG39 furnishes 1,200 to 1,500 gpm for a period of several hours per day.
Wells drilled in nearly every part of the Newala outcrop can be expected to yield between 2 and 5 gpm from depths of less than 200 feet. Well2FF5 was the only one canvassed that could not meet domestic requirements. It is 276 feet deep, penetrated the Newala and terminated in the Knox Group.
Wells supplying the largest quantities of water generally are in low areas and most are near surface streams. Ground water tends to concentrate in large solution channels prior to entering a streambed and, therefore, is available in large quantities.
One potentially hazardous problem that was encountered during the development of a largecapacity well in Cedartown should be considered when selecting sites for future wells. A hole drilled near well 4GG65 was being test pumped at a high rate and appeared satisfactory, when the ground around the well began to subside. Continued pumpage resulted in ground collapse. Thus, in the interest of safety, wells intended for heavy pumpage should be positioned well away from buildings or other permanent structures.
The only part of the Newala outcrop where well yields tend to be lower than average is in a narrow strip along the contact with the Rockmart Slate. The slate overlies the Newala and interferes with the percolation of ground water into the limestone. Solution channels are poorly developed and wells there tend to be poor producers.
Water from wells in the Newala normally is moderately hard to hard. It has a low iron content and rarely is affected by hydrogen sulfide. Water sampled from well 3FF13 had a total hardness of 79 ppm and an iron content of 0.05 ppm.
Only one well, 5FF5, was reported to have water high in iron content. The source of the iron was not determined, but it may be derived from the Deaton Member of the Lenoir Limestone. A small outlier of the Rockmart occurs just across

19

the road from the well and may conceal some Deaton.
Several undeveloped or only partially used springs in the Newala discharge large quantities of ground water of suitable quality for a variety of industrial uses.
Deaton Spring (5GGS4) discharges up to about 15 mgd. However, due to leakage from the main enclosure, the amount of readily available water may be as little as 6 mgd. The spring is located on the south bank of Euharlee Creek just south of the Aragon-Taylorsville road, about two and a half miles northeast of the center of Aragon. It is about a quarter of a mile west of the Seaboard Coast Line Railroad. For year-round use, provisions to protect the spring from flooding by the creek will be required; but as the water discharges from a large cave, it may be possible to tap it while underground, thereby eliminating the need for improvements. A sample of the spring water had a total hardness of 132 ppm and an iron content of 0.09 ppm.
Davitte Spring (5GGS3) discharges about 2.3 mgd from the west bank of Euharlee Creek, a few feet below the Aragon-Taylorsville road, about 2 miles northeast of the center of Aragon. The spring is high enough above the creek to escape most floods, but will require protection from surface water off the road. A sample of the water had a total hardness of 134 ppm and an iron content of 0.08 ppm.
West Spring (3FFS1), about 4 miles southwest of the center of Rockmart, is only a few hundred feet south of U. S. Highway 278 and about the same distance from the Seaboard Coast Line Railroad. It discharges about 1 mgd, but as it is a pool spring and on the valley floor, will require considerable improvement to exclude surface water. Water sampled from the spring had a total hardness of 6 ppm and an iron content of 0.05 ppm.
Hoyt Beck Spring (4GGS3), on the west bank of Fish Creek half a mile south of U.S. Highway 278 and beside the Seaboard Coast Line Railroad, in 1950 discharged about 1 mgd. At present the flow is less than half that amount, but the reduced volume seems to have resulted from clogging of the spring by debris. Cleaning the spring probably will restore the flow. Water from the spring had a total

hardness of 87 ppm and an iron content of 0.06 ppm.
Several other springs discharge from the Newala in Polk County, but their flows are less than 0.3 mgd. Most of these currently are being used for domestic or stock supplies.
Lenoir Limestone
In Polk County the Newala Limestone is succeeded by as much as 35 feet of limestone of Middle Ordovician age that includes two distinct lithologies, herein tentatively correlated with the Lenoir Limestone and its Mosheim Member. The Lenoir Limestone was named by Safford and Killebrew (1876) from Lenoir City, Loudon County, Tenn., and the Mosheim Member was named by Ulrich for the town of Mosheim, Green County, Tenn.
The Lenoir Limestone in Polk County is composed of medium to dark gray, finely crystalline to aphanitic limestone that is thickly to massively bedded where fresh, but upon weathering breaks down into thin slabs and nodular pieces. Some layers of the Lenoir contain a profusion of poorly preserved, largely fragmental fossil material; others are barren of fossils. Maclurites sp. occurs sparingly throughout much of the limestone and locally is abundant. Several specimens of Maclurites sp. were collected from the beds of Lenoir that crop out along the north shore of the small lake that lies just south of the rock quarry, 2.0 miles northnortheast of the center of Rockmart and 1.0 mile east of Georgia Highway 101 (U.S.G.S. Colin. No. 4128-CO).
Mosheim Member
The Mosheim Member, which occurs at different levels within the Lenoir, is mainly light to mediumgray, generally aphanitic limestone, though some is finely crystalline. Except where it is highly cleaved, the Mosheim is massively bedded and, unlike the Lenoir, remains so during weathering. Two unusual features of the Mosheim set it apart from most limestone in the area. One is its tendency to develop a thick chalky crust where it weathers beneath a soil cover. The other is the presence of abundant small, clear calcite crystals scattered throughout the aphanitic groundmass. The only

20

other limestone in the area containing crystals of this type are a few aphanitic layers of the Newala Limestone.
Much of the Mosheim is very fossiliferous. Limestone long exposed at the surface commonly exhibits cross sections of calcareous gastropods, and rock recently uncovered from beneath a soil layer may have calcareous gastropods protruding from its surface or preserved in a chalky crust. Numerous gastropods were collected from the limestone lying along the north side of the large quarry (now filled with water) that is beside Georgia Highway 101, just north of Rockmart. Dozens of gastropods were taken from the pinnacles of Mosheim that were exposed by iron mining, 2.1 miles north-northeast of the center of Rockmart and 1.1 miles east of Georgia Highway 101 (U.S.G.S. Colin. No. 4128-CO). This collection included Loxoplocus (Lophospira) sp., Liospira sp. or possibly badly mashed Clathrospira, Clathrospira sp.,? Raphistoma sp., Trochonema sp., and Helicotoma sp. (see plate 2).
The gastropods taken from the Lenoir Limestone and its Mosheim Member have been distorted by cleavage and pressure, so that even the best cannot be identified to species level. However, Yochelson states that collectively this fauna definitely is later than Early Ordovician and, as it underlies the Rockmart Slate, necessarily is of Middle Ordovician age.
Distribution.-The Lenoir Limestone has been recognized in the vicinity of Rockmart, Aragon, and Taylorsville, Polk County. Limestone immediately beneath the Rockmart Slate south of Cedartown exhibits cross sections of high spired gastropods and probably is Lenoir. Helicotoma sp. collected near Oremont indicates that the formation is present on the west side of the county.
The Lenoir is well exposed in the large quarry at Portland and at several places along the base of ridges made up by Rockmart Slate. Isolated outcrops occur beside the Aragon-Taylorsville road. Several feet of Lenoir Limestone remain along thenorth rim of the quarry beside Georgia Highway 101~ just north of Rockmart. The limestone also is well exposed in and near the quarry about 2 miles north-northeast of the center of Rockmart.
Utilization.-Until the 1950's, when the quality requirements became more stringent, the Lenoir

was extensively used in the manufacture of cement. A large quantity of the limestone was removed from the quarry beside Georgia Highway 101, just north of Rockmart. The formation there is preserved in an overturned or faulted northeast trending syncline. Quarrying began on the northwest limb of the syncline, and followed the formation down dip.
The Lenoir presently is being quarried, along with the Rockmart Slate, about 2 miles northnortheast of the center of Rockmart. The limestone and slate are on the north limb of the same syncline.
A large quantity of Lenoir, along with the Newala Limestone, was taken from the big quarry at Portland and used to make cement.
The most recent attempt to develop the Lenoir for use in cement production was made in the valley about 1.5 miles north of Aragon. An exploratory opening there revealed that the formation is about 25 feet thick and it is covered by nearly 20 feet of overburden. The limestone was found to be too thin for quarrying by itself, and the underlying Newala is too dolomitic to use.
The Lenoir Limestone 1.5 miles north of Aragon occupies an unusual structural position. It underlies the floor of a valley and is nearly horizontal, yet it is flanked on the east and west by fairly high ridges of older Newala Limestone. The latter dips away from the valley in both directions, suggesting that the Lenoir forms the core of an anticline, and this fact has led some workers to conclude that the Lenoir was a lower part of the Newala. In fact, however, the Lenoir has been faulted downward on both sides in a graben.
Prospecting for a suitable quarry site in the Lenoir is complicated by the fact that the formation varies so greatly in thickness. At the Deaton mine, for example, the formation is absent, whereas at Portland, a mile and a half away, it is about 35 feet thick. Even though the limestone is known to be present at most places at the base of the Rockmart Slate, exposures generally are so poor that its thickness cannot be determined without exploratory drilling. Furthermore, the overlying slate normally creates a prohibitive amount of overburden.

21

Away from the main body of the Rockmart Slate, the Lenoir is preserved in appreciable thicknesses only in synclines or where, until recent times, it was protected from solution by a covering of slate. Thus, the limestone generally is associated with outliers of Rockmart, as it is in the quarry about 2 miles north-northeast of the center of Rockmart.
Hydrology.-The Lenoir Limestone is so thin that wells generally penetrate it and derive water from the underlying Newala. A few wells beginning in the Rockmart Slate obtain 5 to 10 gpm from limestone close below, possibly from the Lenoir.
Deaton Member
The Lenoir Limestone locally is overlain by varying thicknesses of iron-rich rocks herein named the Deaton Member of the Lenoir Limestone. The Deaton rests variously on the Lenoir, its Mosheim Member, or in the Deaton iron mine where these two have been eroded, directly on the Newala Limestone. The name Deaton originally was applied to these rocks by Spencer (1893, p. 83) because they were well exposed in the Deaton iron mine, about 2 miles west of Taylorsville. Spencer included the Deaton within the Newala Limestone (his Chickamauga Limestone) and correlated it with the iron ore at about the same stratigraphic position in Whitfield County, Ga., and with Safford's (1869) iron limestones of Tennessee. Hayes (1902) considered the Deaton to be in the lower part of the Rockmart Slate.
Lithology and distribution.-The Deaton Member has been recognized only in a relatively narrow zone of eastern Polk County near Rockmart and Taylorsville. It occurs as isolated exposures within this small area, and its character varies greatly from one outcrop to another, especially across the strike; thus the unit is assigned member status.
At the Deaton mine, one of its more westerly exposures, the Deaton consists of more than 100 feet of dark-gray to nearly black calcareous ore in beds 0.5 to 4 feet thick, some of which contain about 30 percent iron. Much of the ore is magnetic, due to a high magnetite content. Decalcification and oxidation produce pieces of dark-brown limonitic ore and deep red hematitic ore that accumulate in a thick red sandy clay soil. Some of the ore has a high sand and silt content and weathers to brown and red ferruginous sandstone

and siltstone.
Interbedded with the highly ferruginous beds are layers of conglomerate made up of pebbles and a few cobbles of dolomite, limestone, some sandstone and siltstone, and small pieces of dark shale, in a matrix of ferruginous, chlcareous ,feldspathic sandstone. A high percentage of the pebbles are siliceous dolomite that, in weathered rock, leave a residue resembling pisolites or oolites. Round voids in the rock are left by solution of the limestone pebbles. The pebbles apparently were derived mainly from the Newala and the Lenoir Limestones, and the Knox Group, which were uplifted and subjected to erosion during the time the Deaton was being deposited.
Ore of the Deaton Member has been mined from pits about 2 miles northeast of the center of Rockmart where, as recently as 1955, the iron was used in the manufacture of cement. No fresh ore is exposed there but the deep red soil contains scattered pieces of brown, red, and yellowish argillaceous and feldspathic sandstone and siltstone. Some of these pieces contain spherical silt and clay inclusions that appear to be the remains of siliceous dolomite pebbles similar to those occurring in the rock at the Deaton mine; other pieces include spherical hollows that probably contained limestone pebbles. Pinnacles of the Mosheim Member are exposed in the bottom of the pits northeast of Rockmart and show that the Deaton at this locality was deposited on slightly younger limestone than it was at the Deaton mine. These workings are near what Hayes' map (1902) shows as the settlement of Red Ore, and it seems likely that the red ore here may be what Hayes (1902, p. 3) referred to as being in the lower part of the Rockmart Slate. The Rockmart is present only a short distance to the east.
About 5 miles east of the Deaton mine, near the Polk-Paulding County line, the Newala Limestone is succeeded by medium to very coarse grained, feldspathic quartzite, sandstone and quartz-pebble conglomerate, at least 25 feet thick but probably much thicker. The massively bedded quartzite forms a prominent ridge between the Newala Limestone and the Rockmart Slate . Similar outcrops occur close to the Bartow-Paulding County line about a mile farther northeast. Although the quartzite has a character very different from the limestone in the Deaton mine, its stratigraphic position indicates that it is correlative with the Deaton Member.

22

Just south of U.S. Highway 278 about 2% miles southeast of Van Wert, the Deaton consists of medium-grained rusty-weathering sandstone and quartzite, probably about 10 to 20 feet thick, that does not seem to be especially ferruginous. It rests on the Newala or possibly some Lenoir Limestone, and seems to be immediately overlain by the Rockmart Slate, although the upper contact is not exposed.
Spencer (1893, p. 169) states that the Deaton also occurs about 1.75 miles northeast of the center of Rockmart and 0. 75 mile southeast of Van Wert, but the writer did not find exposures there. Spencer also reported an occurrence of the Deaton a mile southeast of Van Wert, but this deposit of ferruginous material is very small and as it occurs well up in the Rockmart Slate, it does not appear to be related to the Deaton.
Fauna and age.-The few fossils known from the Deaton Member are fragmentary and poorly preserved. Those found all came from the Deaton mine (abandoned), south of the paved road about 2 miles west of Taylorsville, Polk County (U.S.G.S. CoHn. No. 6700-CO). A sample of brown, ferruginous rock taken from the south edge of the mine contained shell fragments that G. A. Cooper, U. S. National Museum, identified as probably a linguloid brachiopod. Also present in the rock were 2 poorly preserved conodonts that John W. Huddle questionably referred to Drepanodus, a genus common in the Ordovician but known from the Cambrian and probably occurs in younger rocks.
The fossils suggest that the Deaton was an estuary deposit laid down in brackish water.
The stratigraphic position of the Deaton between the Lenoir Limestone and the Rockmart Slate shows that it is of Middle Ordovician age.
Hydrology.-The Deaton Member is so thin and occurs so sporadically that it has little importance as an aquifer. Wherever the Deaton might yield water, it should be cased off to prevent contamination of the supply by iron.
Rockmart Slate
The Rockmart Slate of Middle Ordovician age was named by Hayes (1891, p. 143) for the town of Rockmart, Polk County, Ga., near where the slate is exposed in several quarries. The Rockmart unconformably overlies the Newala and Lenoir

Limestones and locally the Deaton Member of the Lenoir. It is succeeded unconformably by the Armuchee Chert or the Frog Mountain Sandstone in western outcrops, and by the Fort Payne Chert and possibly some Armuchee Chert in eastern outcrops. The name Rockmart Slate as used in this report has been adopted by the U. S. Geological Survey.
The type section of the Rockmart Slate is along the Seaboard Coast Line Railroad beginning in the south part of Rockmart and continuing southeastward across U. S. Highway 278 and about 1 mile beyond that highway to the upper contact of the formation with the Fort Payne Chert. This section includes 2 separate exposures of the lower part of the Rockmart. One is in the south part of the town of Rockmart, and the other is between Van Wert and where the railroad crosses U. S. Highway 278. The upper part of the Rockmart is exposed intermittently along the railroad east of U. S. Highway 278.
One reference section for the Rockmart Slate is along the Southern Railway east of Rockmart, where slate of the lower part and sandstone, slate, and conglomerate of the upper part of the formation are exposed in cuts. Another reference section is along the unpaved road going east out of Van Wert to Braswell. This road crosses hills and ridges made up of both the lower and the upper parts of the Rockmart.
Lithology.-The Rockmart consists chiefly of clay and silt slate but it also includes large quantities of nonfissile siltstone, sandstone, and conglomerate. The slate forms a broad sheet of fairly uniform thickness that extends essentially unbroken across the entire outcrop belt of the formation. The sandstone, siltstone and conglomerate farm a wedge, thickest to the southeast, that overspreads the slate as far west as Cedartown.
The most common type of slate in the Rockmart, and the one dominating the lower part of the formation, is dark-gray to nearly black, calcareous, fairly pure clay slate. It has well developed cleavage on the eastern side of the county, especially near Rockmart, and moderate cleavage in most other areas. Upon exposure, the slate first becomes lighter gray; some of it then alters to tan or yellowish brown, commonly with an orange tint, and finally to pink. Other weathers to greenish or light olive gray, then to tan, and finally to pink, the latter

23

type being most common on the west side of the outcrop belt. The weathered slate breaks down into soft, very thinly laminated waxy flakes. Slate of this type is abundantly displayed across the entire outcrop belt and can be observed in numerous quarries and prospect pits.
Another important constituent of the Rockmart is argillaceous and micaceous siltstone. Some of the siltstone is thickly bedded and has a uniform tan color. Some other is made up of 1/8 inch to 1/2 inch thick beds of slightly differing composition that weather to various shades of brown and yellow, giving the rock a fine color banding. Some siltstone has poorly developed cleavage and splits into slabs about a, quarter of an inch thick, but most tends to remain massive and does not separate into layers, either along cleavage or the bedding. The highly weathered rock disintegrates into small irregularly shaped pieces.
Siltstone is well displayed beside the u npaved road three-quarters of a mile northwest of the intersection of Georgia Highway 100 and U. S. Highway 27.

The sandstone in the Rockmart is light to medium gray and ranges in grain size from very fine to very coarse. The grain size increases from west to east across the county, although both fineand coarse-grained varieties are present in most areas. Bedding likewise tends to thicken toward the east. Near Rockmart some beds reach a thickness of more than 6 feet, whereas in the Cedartown area they generally are less than 1 foot thick, though beds 3 or 4 feet thick do occur. As a rule, the sandstone is interbedded with slate or conglomerate so that unbroken thicknesses of sandstone rarely exceed 10 feet.
Nearly all of the sandstone in the Rockmart is feldspathic, which sets it apart from other formations in the area except the Frog Mountain Sandstone. The weathered rock is tan to rusty brown and has an interior flecked with cream-colored or light-brown inclusions remaining from the weathered feldspar.
Sandstone is well exposed along the Seaboard Coast Line Railroad southeast of Van Wert. Uncommonly thick-bedded sandstone crops ou t at the top of the large cut on the Southern Railway about

Figure 6. Conglomerate in the Rockmart Slate. 24

2 miles east of Rockmart. It occurs at several places along the unpaved road going east out of Rockmart toward Braswell, and crops out on the east flank of Signal Mountain, and on several ridges south and east of Rockmart.
Conglomerate in the Rockmart consists of several types . One of the most wide spread types is made up of pebbles and cobbles of limestone, dolomite, slate, sandstone, chert, and both sedimentary and metamorphic quartzite, generally in that order of abundance, incorporated in a matrix of feldspathic sandstone (fig. 6 ).
The pebbles and cobbles are composed of material derived from older Paleozoic formations and some transported by streams from the Piedmont. Most of the limestone and dolomite can be recognized as coming from the Newala and Lenoir Limestone and the Knox Group. Still other dolomite is similar to that of the Shady Dolomite. Reddish sandstone from the Rome Formation is present, as is quartzite and sandstone from the Rome or possibly from the Weisner Quartzite. The chert probably came from the Kn_ox proup and the Newala Limestone. Some of the sandstone and shale is reworked Rockmart. Other conglomerates are composed of pebbles of essentially the same material but have a matrix of sandy slate, graywacke, clay slate, or rarely dolomite or limestone.
Weathering dissolves the carbonate from the conglomerate leaving layers of rusty-brown sandstone or other matrix material pocked with rounded hollows.
Outcrops of the above types of conglomerate are not numerous in the Cedartown area. One good exposure, although several hundred feet from the road, can be seen on the south side of the ridge, about three-quarters of a mile southwest of the intersection of U. S. Highway 27 and Georgia Highway 100.
Several conglomerate beds are exposed in the broad expanse of the formation south of Grady. One is beside the unpaved road near the crest of a low ridge, about half a mile northwest of Antioch School.
Another type of conglomerate in the Rockmart is composed of fme quartz pebbles in a matrix of feldspathic sandstone. It is exposed near the top of the formation along Georgia Highway 100, south

of the junction with U.S. Highway 27.
The conglomerate bodies are lenticular and rarely extend more than a few hundred feet in any direction before pinching out or grading into sandstone or conglomeratic slate. The pebbles and cobbles probably were brought in by streams and dumped into a shallow sea where they accumulated near shore. The conglomerate lenses in the south easternmost outcrops are thickest and have the widest lateral extent. They also contain the coarsest and the least rounded pebbles and cobbles, apparently having been deposited nearest the source area.
Conglomerate outcrops are numerous near Rockmart. Several are present on the north slope and near the crest of the ridge about 2 miles southwest of the center of Rockmart. Conglomerate is prominently displayed along the Seaboard Coast Line Railroad east of the overpass on U.S. Highway 278. It also occurs in the cut of the stream flowing just west of U. S. Highway 278, at the curve 0.4 mile south of the same overpass. Thil:k beds of sinuously folded conglomerate have been uncovered in the large cut of the Southern Railway 2 miles east of Rockmart. Conglomerate having a dolomitic matrix occurs beside the road that runs along the south side of Lake Dorene, south of Rockmart. Conglomerate is present on the east slope of Signal Mountain and in the valley east of the mountain.
The pebbles and cobbles in most exposures of the conglomerate have been greatly elongated parallel to the cleavage, so that their diameter prior to deformation is difficult to determine . In the Cedartown area most of the pebbles appear to have been between 1 and 2 inches in largest dimension mixed with only a few small cobbles. South of Grady, pebbles were about the same size and the cobbles were as much as 4 inches across. In the Rockmart vicinity, pebbles also occurred, but the cobbles which were far more abundant, ranged from 3 to 6 inches in greatest dimension and a few were nearly a foot across.
Distribution.-The Rockmart extends for a distance of about 30 miles along the southern and eastern margins of the unaltered Paleozoic rocks in Pol!-- County, expanding into large areas south of Cedartown and Gray, in the vicinity of Rockmart, and between there and Taylorsville. Two isolated outcrops also occur in the adjacent part of Bartow County. Middle Ordovician slate in Cherokee

25

County, Ala., was included within the Rockmart Slate by Hayes (1894, p. 472), but it currently is considered part of the Athens Shale by the Geological Survey of Alabama.
Age of the Rockmart Slate.-Geologists long have disagreed over the exact age of the Rockmart. Beginning with his earliest work in Georgia, Hayes (1891, 1902) assigned the Rockmart to the Ordovician (Silurian of his day) and correlated it with the upper part of the Chickamauga Limestone north of the Coosa Fault. Spencer (1893), Veatch (1909), and McCallie (1910) in general agreed with Hayes, but Ulrich (1911) assigned the Rockmart to the Lower Ordovician Blount Group (upper Chazy) of former usage and correlated it with the Athens Shale of Tennessee. Maynard (1912) followed Hayes' thinking and LaForge (1925) showed the Rockmart as Middle Ordovician in age, but does not indicate whether it includes any Lower Ordovician. Butts and Gildersleeve (1948), on the other hand, placed the Rockmart in the Mississippian System, correlating it with the Floyd Shale, and it is shown as that age on the geologic map of Georgia (Cooke and others, 1939).
This lack of agreement among geologists concerning the exact age of the Rockmart developed because fossils from this formation were unknown except to early workers. According to Robert A. Laurence (oral communication, 1964), who found the information recorded in a field notebook, graptolites were discovered near the base of the Rockmart in 1890 by M. R. Campbell while he assisted Hayes in mapping the Rome and Tallapoosa quadrangles. For some reason, though, the find was not reported, and later workers were unaware of Campbell's discovery. Fossils were not again reported from the Rockmart until the present investigation.
Although Butts and Gildersleeve (1948, p. 53) reported finding fossils of Mississippian age in the Rockmart, these fossils now are known to have come from the Fort Payne Chert. The fossils Butts collected were in chert exposed in the road metal pits beside Georgia Highway 100, half a mile south of the junction with U. S. Highway 27. The chert is steeply dipping, and it is underlain and overlain by slate and sandstone of similar character. Butts identified the slate above and below the chert as Rockmart, and therefore concluded that the chert and the slate were part of the same formation Indeed, the slate beneath the chert is Rockmart,

but that above it belongs to the Floyd Shale of Mississippian age. The fossils Butts found came from the Fort Payne Chert which overlies the Rockmart Slate.
Fauna.-During the present investigation, several hundred graptolites were collected from the Rockmart Slate throughout its entire outcrop belt. The fossils came from clay slate, silty slate and nonfissile siltstone. On the western side of the county, where the formation is mostly slate, the graptolites are found to be fairly well distributed throughout the entire section. In the Grady and Rockmart areas, on the other hand, they are limited to the lower half or so of the formation and in every instance occur below the sandstone-conglomerateshale sequence which constitutes the middle and upper parts. The possible significance of this fact is discussed later in the section on correlation of the Rockmart.
Graptolites were collected exhaustively from nine localities in Polk County. The species obtained from each locality (table 4) are listed and discussed collectively in the text, and some are pictured in plate 1. In addition, graptolites were collected from one place in the Athens Shale of Murray County, Ga., to determine possible correlations of the Athens Shale and the Rockmart Slate; these are listed under locality number 10. Graptolites collected by Preston E. Cloud, Jr., from the Athens Shale of Cherokee County, Ala., shown as locality number 11, are listed and discussed collectively in the text.
William B. N. Berry identified the graptolites and made all of the age determinations. The zone numbers used are those of Berry (1960).
Locality number 1: From slate just below sandstone and chert at northwest end of small upper dam at Elders Lake. Climacograptus cf. C. riddellensis Harris Climacograptus n. sp. (of the type of C. marathonensis) Cryptograptus schaferi Lapworth Glyptograptus aff. G. teretiusculus var. siccatus (Ellis and Wood) Retiograptus ? sp. Age: Middle Ordovician-in the interval of Zone 10 (Glyp tograp tus teretiusculus Zone) into Zone 12 (Climacograptus bicornis Zone)-proba-

26

bly the Glyptograptus teretiusculus Zone (Zone 10). Stratigraphic position: This collection is from the top of the formation.
Locality number 2: From silty slate in the spillway at the southeast end of small upper dam at Elders Lake. Cryptograptus tricornis (Carruthers) dkhograptid fragments Glossograptus sp. Glyptograptus euglyphus (Lapworth) Glyptograptus aff. G. euglyphus var. sepositus (Keble and Harris) Age: Middle Ordovician-in the span of Zone 9 (Hallograptus etheridgei Zone) to Zone 12 (Climacograptus bicornis Zone)-probably Zone 10 (Glyptograptus teretiusculus Zone) Stratigraphic position: This collection may be from the middle or upper part of the formation but this is uncertain due to the close proximity of faulting.
Locality number 3: From slate and shale about 30 feet east of unpaved road at curve, 3.06 miles east of Old Brewster School and 0.65 mile southeast of Pine Bowers Church. Climacograptus cf. C. riddellensis Barris Climacograptus cf. C. scharenbergi Lapworth Climacograptus n. sp. (like C. marathonensis) Climacograptus sp. Cryptograptus tricornis (Carruthers) Didymograptus cf. D. paraindentus Berry Didymograptus cf. D. tornquisti Reudemann dichograptid fragments Glossograptus ciliatus Emmons? Glossograptus hincksii (Hopkinson) Glyptograptus euglyphus (Lapworth) Glyptograptus euglyphus cf. var. sepositus (Keble and Harris) Glyptograptus cf. G. teretiusculus (Risinger)
Glyptograptus aff. G. teretiusculus (Hi-
singer) Glyptograptus cf. G. teretiusculus var.

siccatus (Ellis and Wood) Retiograptus sp. Age: Middle Ordovician-Zone 10 (Glyptograp tus tere tiuscu lus Zone) Stratigraphic position: The position of this collection in the formation is uncertain but it probably is in the lower half.
Locality number 4: From slate in ditch on north side of unpaved road, 3.1 miles east of Old Brewster School and 0.75 mile southeast of Pine Bowers Church. Climacograptus riddellensis Harris? dichograptid fragments Glossograptus sp. Glyptograptus aff. G. euglyphus (Lapworth) Glyptograptus sp. Hallograptus inutilis (Hall) Isograptus sp. (of the I. caduceus type) Age: Middle Ordovician-in the interval of Zone 9 (Hallograptus etheridgei Zone) to Zone 10 (Glyptograptus teretiusculus Zone) Stratigraphic position: Located very close to fault, so position is uncertain.
Locality number 5: From slate exposed in the ditch on the west side of the paved road 4. 9 miles southsouthwest of the center of Cedartown and 0.6 mile south of Pine Bowers Church, 100 to 200 feet south of locality number 8. Climacograptus riddellensis Harris Climacograptus aff. C. riddellensis (Harris) dichograptid fragments Didymograptus cf. D. robustus var. norvegicus Berry MS Glossograptus sp. Glyptograptus euglyphus (Lapworth) Glyptograptus sp. Pterograptus n. sp. (similar forms occur in the Australian Darriwil Glyptograptus teretiusculus Zone) Retiograptus aff. R. speciosus Harris Age: Middle Ordovician-Probably Zone 10 (Glyptograptus teretiusculus Zone) although it might be Zone 9 (Hallograptus etheridgei Zone). Stratigraphic position: Uncertain.
27

Locality number 6: From siltstone on the north bank of the unpaved road 3.10 miles south-southwest of the center of Cedartown and 0.72 mile northwest of the intersection of U. S. Highway 27 and Georgia Highway 100. Glyptograptus euglyphus Glyptograptus cf. G. teretiusculus var. siccatus (Ellis and Wood) Age: Middle Ordovician-in the interval of Zone 9 (Hallograptus etheridgei Zone) to Zone 11 (Nemagraptus gracilis Zone) possibly Zone 10 (Glyptograptus teretiusculus Zone) Stratigraphic position: Middle of formation.
Locality number 7: From silty slate on the north side of the operating slate quarry just north of the Seaboard Coast Line Railroad, in the southern part of Rockmart. This is the locality in which M. R. Campbell made the original discovery of graptolites in the Rockmart Slate in 1890. Climacograptus sp. (of the C. riddellensis type) Glossograptus sp. Glyptograptus euglyphus (Lapworth) Age: Middle Ordovician-in the interval of Zone 10 (Glyptograptus teretiusculus Zone) to Zone 12 (Climacograptus bicornis Zone). Stratigraphic position: Lower part of the formation.
Locality number 8: From highly weathered slate beneath layers of chert in the west cut of the paved road at the intersection with the dirt road, 4.9 miles south-southwest of the center of Cedartown and 0.5 mile south of Pine Bowers Church. (U.S.G.S. Colin. No. D1092-CO). Glyptograptus euglyphus (Lapworth) Climacograptus cf. C. scharenbergi Lapworth Trigonograptus sp. Glyptograptus sp. Glyptograptus aff. G. teretiusculus (Risinger)

Glyptograptus ? sp. Glyptograptus ? sp. or possibly Ortho-
graptus ? sp.
Glyptograptus cf. G. euglyphus var. sepositus Harris and Keble
Climacograptus sp. (of the C. angulatus Bulman type)
Hallograptus cf. H. mucronatus (Hall) Cryptograptus schaferi Lapworth Retiograptus sp. Age: Middle Ordovician-Nemagraptus gracilis Zone (Zone 11) possibly - though it might be Glyptograptus teretiusculus Zone (Zone 10) or as young as Climacograptus bicornis Zone (Zone 12). Stratigraphic position: Upper part of formation, probably at the top.
Locality number 9: From slate in cut of unpaved road 5.50 miles southwest of the center of Rockmart and 4.20 miles south of U. S. Highway 278 (U.S.G.S. Colin. No. Dl093-CO.). dichograptid fragment Climacograptus aff. C. riddellensis Harris Glossograptus sp. Glyptograptus euglyphus (Lapworth) Glyptograptus cf. G. teretiusculus (Risinger) Glyptograptus euglyphus (Lapworth) Age: Middle Ordovician-probably Glyptograptus teretiusculus Zone (Zone 10) this age is based on the joint occurrence of a Climacograptus of the C. riddellensis type with glyptograptids of the G. teretiusculus and G. euglyphus kinds. The total age span possibly could be as young as Zone 12 (Climacograptus bicornis Zone). Stratigraphic position: near the base of the Rockmart.
Locality number 10: From the Athens Shale, Murray County, Ga., at or near the base, just off the west slope of Sumack Ridge, 7.0 miles slightly west of north from the center of Chatsworth, 1.5 miles west of the east edge of the Dalton quadrangle, and f.25 miles east of the Cleveland Road (U.S.G.S. Colin. No. D1371-CO).
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Glyptograptus aff. G. teretiusculus var. siccatus (Ellis and Wood)
dichograptid fragment Glyptograptussp. Glyptograptus ? sp. Glyptograptus aff. G. teretiusculus (Ris-
inger) dichograptid fragment Glyptograptus cf. G. teretiusculus (Ris-
inger) Glyptograptus cf. G. euglyphus (Lap-
worth) Retiograptus cf. R. speciosus Harris
[This specimen is identical to some from a highest Darriwil age locality (Glyptograptus teretiusculus Zone) in Victoria, Australia. Retiograptus sp. Climacograptus cf. C. riddellensis Harris Climacograptus n. sp. (of the C. mara-
thonensis type) dichograptid fragment and Cryptograp-
tus ? sp. biserial scandent form? Age: Middle Ordovician-Glyptograptus
teretiusculus Zone (Zone 10) probably although the age might be as young as the Climacograptus bicornis Zone (Zone 12). Again, the joint _association of climacograptids like C. riddellensis with G. teretiusculus and G. euglyphus kinds of glyptograptids and a Retiograptus like R. speciosus strongly suggest a Zone 10 age interpretation. Stratigraphic position: at the base of the Athens Shale.
According to Berry this collection appears to be slightly older than, or possibly the same age as Collection D1092-CO from the Rockmart Slate. It is probably the same age as Collection D1093-CO from the Rockmart Slate.
Locality number 11: Collected by P. E. Cloud, Jr., from the Athens Shale in Cherokee County, Ala., on the west bank of the paved road 0.88 mile southwest of the highest elevation of Frog Mountain near the west edge of the Rock Run and vicinity, Ala.-Ga. quadrangle. Climacograptus sp. (thecae like those of

C. luperus) Climacograptus sp. (a slender form with
thecae like those of C. riddellensis ) Didymograptus? sp. Glossograptus sp. Glyptograptus cf. G. euglyphus (Lap-
worth) Glyptograptus sp. Age: Middle Ordovician-in the interval of Zone 9 (Hallograptus etheridgei Zone) to Zone 12 (Climacograptus bicornis Zone) at a guess - Zone 10 (Glyptograptus teretiusculus Zone) based on the association of climacograptids with pouched thecae with Glyptograptus cf. G. euglyphus. Stratigraphic position: apparently near the top of the Rockmart; near the contact with overlying chert.
Regarding collections from localities 1 through 9, Berry states, "Those collections that include more than two or three forms seem to come from Zone 10. Climacograptids like C. riddellensis which have deeply pouched thecal excavations and a zig-zag suture appear initially in Zone 10 in North America-and at a correlative position in Australia. Their association with retiograptids which are similar to the Australian highest Darriwillian retiograptids, Glyptograptus euglyphus, and small forms of the Glyptograptus teretiusculus type strongly suggest a Zone 10 age assignment. The collections in which two or more of these occur together (Locality numbers 1 through 7 and 11) are probably all of Zone 10 age. Because stratigraphic ranges of graptolites in the southern Appalachians are not well known, and because the precise diagnostic association of Zone 10 is also not well known, the age interpretation of the collections is open to some question and thus the possible age span for each has been noted. The correlation of Zone 10 with the brachiopod Stage sequence is not certain, but I suggest about an Ashby correlation." Berry is referring to the Ashby Stage of Cooper (1956).
Graptolites collected thus far show that the lower part of the fossiliferous Rockmart Slate falls in the interval of Zone 9 to Zone 10, and probably is Zone 10. The middle and apparently most of the upper part are in the interval of Zone 10 to Zone 12, and probably are of Zone 10 age, as well.

29

The uppermost beds of the Rockmart at one locality south of Cedartown yield graptolites believed to be of Zone 11 age.
Correlation.-Assuming that the age assignments given the graptolite assemblages prove correct in light of further collection, the bulk of the fossiliferous part of the Rockmart is slightly younger than the Deepkill Shale (Early and Middle Ordovician) of New York, but is older than the Athens Shale (Middle Ordovician) at Athens, Tenn. Only the uppermost part of the Rockmart carrying Zone 11 fossils is correlative with the Athens Shale in Tennessee, or with the Athens Shale south of Birmingham, Ala., which Cooper (1956, p. 57) has named the Columbiana Formation.

. It is the writer's belief, however, that as the clastics at the top of the Rockmart form a distinct lithologic unit, they should be separated from the Rockmart and designated as a formation. The conglomerate and sandstone in the unit are remarkably similar to those in Murray County, Ga.,mapped by Butts and Gildersleeve (1948) as the Tellico Formation, and by Salisbury (1961) as the Chota Formation. The conglomerate is nearly identical to that in the Tellico Formation in Georgia and in Tennessee described by Kellberg and Grant (1956).
Further investigation may provide evidence for correlating the clastics at the top of the Rockmart with at least part of the sandstone-conglomerateshale sequence mapped as Tellico and Chota in Murray County, Ga.

A collection of graptolites (locality 10) from the basal beds that have been mapped as Athens Shale in Murray County, Ga. (Butts and Gildersleeve, 1948), and called a southern extension Paperville by Cooper (1956, p. 53), is in the range of Zone 10 to Zone 12. Berry believes they may be Zone 10 or that they possibly may be Zone 11. If the Zone 10 age proves correct, the base of the so-called Athens Shale in Murray County, Ga., is the same age as the Rockmart; if it is Zone 11 age, the shale is the same age as the Athens Shale of Tennessee.
Slate cropping out over a broad area of Cherokee County, Ala., initially was mapped as Rockmart by Hayes (1894, p. 472), but more recently it has been considered as Athens Shale (Butts, 1926; Cloud, 1967). Graptolites taken from near the top of the slate by P. E. Cloud, Jr., about 10 miles west of Polk County, show that it falls in the interval of Zone 9 to Zone 12, and Berry believes it is Zone 10. If so, the slate is the same age as the Rockmart Slate, but is older than the Athens Shale farther southwest in Alabama. Because the slate is physically continuous with and lithologically identical to the Rockmart, it should be considered part of the Rockmart.
The lower, predominantly slaty part of the Rockmart, beginning near Cedartown in Polk County, is overlain by an eastward thickening wedge of clastics, composed largely of sandstone, conglomerate, and conglomeratic slate. The clastics consitute a mappable unit, and where sufficiently thick, are delineated on the accompanying geologic map, but they are included in the Rockmart for want of fossil evidence to determine their exact age.

Thickness.-In Polk County, the Rockmart ranges in thickness from 0 to about 600 feet. East of Van Wert, where it contains the largest amount of clastic material, the formation attains a maximum thickness of between 400 to 600 feet. North and west of this area, as the proportion of clastic material decreases, the Rockmart thins to between 200 and 300 feet and remains about that thick across the county to the Alabama line near Esom Hill. At Etna, where the Rockmart re-enters Polk County from Alabama, it is between 200 and 300 feet thick, but it thins toward the east, diminishing to about 20 feet at Oremont, and it is absent a quarter of a mile southeast of there, apparently having been eroded off an anticline that formed prior to deposition of the Frog Mountain Sandstone of Early and Middle Devonian age.
It is interesting to note that past workers have considered the Rockmart's thickness to be far greater than 600 feet. For example, Spencer (1893) showed it to be 1,200 feet thick and Butts and Gildersleeve (1948) gave its thickness as 3,000 feet. It is not known how they arrived at these estimates, but it seems possible they may have been influenced by the pseudostratification produced by cleavage on the slate and conglomerate southeast of Van Wert where the Rockmart is a mixture of slate, limestone-pebble conglomerate, and a little sandstone, and the entire section is steeply folded. Compressional forces have greatly stretched all of the conglomerate pebbles and oriented their long axes parallel to the dip of the cleavage in the slate. The elongated pebbles and the slaty cleavage are parallel and inclined steeply to the east, so that where they are viewed in limited cross section, as in the shallow cuts of the Sea-

30

Figure 7 Conglomerate layer in the Rockmart Slate showing pebbles stretched with long axes parallel to dip of cleavage.

board Coast Line Railroad east of U. S. Highway 278, they have the appearance of successive bedding (fig. 7). This apparent stratification is exposed for thousands of feet across the strike and conveys the impression that the formation has great thickness.
An examination of the thin sandstone beds present in the section, however, reveals that the formation along the railroad track is folded and that the same beds of conglomerate and slate are repeated several times. The apparent stratification is solely the result of cleavage (fig. 8).
A similar sequence of slate, sandstone, and conglomerate is exposed in the big cut of the Southern Railway 2 miles east of Rockmart. In this cut the conglomerate pebbles also are stretched and have their long axes oriented parallel to the dip of the cleavage in the slate, but because the cut is high and the sandstone beds are thicker, it is easy to see that the fonnation is gently folded (fig. 9). The Rockmart as a whole is inclined at a shallow angle to the east approximately paralleling the dip of the formations above and below. Thus, the thickness of the Rockmart is reflected fairly

accurately by the corrected vertical distance separating the Newala and Lenoir Limestonebelow the Rockmart and the Fort Payne Chert that overlie it. At most, this distance is about 600 feet.
Hydrology.-Thirty wells inventoried in the Rockmart Slate vary in depth from 26 to 198 feet with an average depth of 98 feet. Yields are reported to range from about 1 gpm to 30 gpm with most wells supplying between 5 and 15 gpm.
The water varies from soft to hard depending on the location and the depths of tQ.e wells. In general, the quality is satisfactory for home use although eight well owners reported their water had an objectionably high iron content. Six of these wells are wholly within the Rockmart, but the other two are close to the edge of its outcrop and probably pass through the slate into the limestone below. They may derive iron from the highly ferruginous Deaton Member of the Lenoir Limestone which occurs at that level. Water from one well in the Rockmart (3FF25) had a total hardness of 105 ppm and an iron content of 2.6 ppm. A sample from well 3FF34 had an iron content of 0.79 ppm, and a total hardness of 398 ppm.

31

The Rockmart is the only formation in the study area that yields water having a high noncarbonate hardness.
The one well inventoried that clearly derives water fr om t he upper sandstone part of the Rockmart yielded about 2 gpm. Other wells beginning in the sandstone are deep enough to pass through it and obtain water from the underlying slate ; their yields tend to be higher. Well 5FF9, which is 150 feet deep, is estimated to yield about 10 gpm, and a sample of the water had a total hardness of 32 ppm and an iron content of 1.1 ppm.
Other Formations of Ordovician Age
In Floyd County, the Ordovician System includes representatives of four or possibly five formations. They are too thin to be shown individually on a geologic map of the scale used with this rep ort (fig. 4) and are shown as a single unit.
According to Butts and Gildersleeve (1948, p. 31 ), the Moccasin Limestone makes up th e main body of rock in the Ordovician System in Floyd County. A more detailed study indicates, h owever,

that only a small part of the section belongs to the Moccasin; the remainder is correlative with other formations of Middle Ordovician age: the Murfreesboro Limestone, the Ridley Limestone, and the Bays Formation. Good exposures of these formations can be seen on Horseleg Mountain ; some of them crop out on the west slope of Simms Mountain, around Heath Mountain, and on Lavender Mountain.
Lithology, distribution, and fauna.-Near the southwest end of Horseleg Mountain, the two limbs of the mountain are connected by a saddle. About 100 fee t south of this saddle the Copper Ridge Dolomite is unconformably overlain by 30 or 40 feet of rock that resemble a part of .the Murfreesboro Lim estone, common farther n orth in the State (Butts and Gildersleeve, 1948, p. 23). The Murfreesboro consists of calcareous m udstone, yellow at the base, but grading upward into pink and finally into red mudstone flecked with yellow.
Abou t 600 feet southwest of the saddle, the lower yellow mudrock of the Murfreesboro apparently is replaced by abou t 50 feet of fairly pure limestone. The limestone rests on the Copper

Figure 8. Beds of sandstone in Rockmart Slate showing divergence of bedding and cleavage. 32

Figure 9. Cuts of the Southern Railway 2 miles east of Rockmart showing folded sandstone beds in Rockmart Slate.

Ridge Dolomite and is overlain by red mudrock that, as far as exposures reveal, is continuous with the red mudrock near the saddle. The limestone is light to medium gray, thickly to massively bedded, and aphanitic t o finely crystalline. Locally it displays pink and green clouding. Fossils in the rock are limited to cross sections of calcified gastropods, so identifications could not be made. The general cparacter of the stone, h owever, and particularly the pin k and green clouding, is suggestive of both the Newala Limestone and the Murfreesboro Limestone in Catoosa and Walker Counties, Ga.
On the south side of the saddle that separates the two limbs of Horseleg Mountain, and about 30 feet above the Upper Cambrian-Middle Ordovician boundary, the mudrock of the Murfreesboro is overlain by several feet of cobbly pink and yellowish-green argillaceous limestone containing specimens of a brachiopod (see plate 2, fig. 2a-c) identified by Robert B. Neuman as Rostricellula variabilis Cooper (U.S.G.S. CoHn. No. 4425-CO). Cooper (1956, p. 654) reported this variable species in Georgia only from the Fascifera bed of Ridley Limestone, and according to Neuman this collection may have come from the same level, but

associated fossils should be collected and studied to confirm this correlation:- Unfortunately none were found. A few very . poorly preserved lowspired gastropods (Maclurites ?) occur slightly higher in comparatively pure blue-gray flaggy limestone that forms the top of the saddle.
Succeeding the flaggy limestone in the saddle is abou t 100 feet of maroon and some yellow, shale and calcareous silty mudstone, mixed with thinbedded reddish siltstone and fine- to mediumgrained sandstone. Also present is a little pink and red and, rarely, blue impure limestone. This section probably is correlative with the Moccasin Limestone as suggested by Butts and Gildersleeve (1948, p. 31).
The remaining 300 feet of the Ordovician include lithologies that correspond closely to the Middle Ordovician Bays Formation, and may include some Sevier Shale and possibly rocks of Upper Ordovician age. The sequence is composed of yellow, maroon, and reddish shale and calcareous mudstone, thin-bedded red siltstone, and impure fine to very coarse grained sandstone. The middle and upper parts include beds of light gray

33

rather clean quartzite that are thin bedded and finer grained below, becoming very massively bedded and coarser grained toward the top. Some quartzite layers are conglomeratic, containing rounded quartz pebbles as much as a quarter of an inch across. A 5-foot layer of altered volcanic ash occurs near the middle of the unit; it is exposed in the west ditch of the road on top of Horseleg Mountain a little less than a mile southwest of the fire lookout tower.
The basal beds of Ordovician rocks on Horseleg Mountain are separated from the underlying Knox Group by a major unconformity. This unconformity is marked by a bed of conglomerate from 6 inches to about 2 feet thick composed of rounded and angular pieces of detrital chert ranging from sand size to about half an inch in greatest dimension, cemented by a matrix of mudstone or limestone. The matrix is identical to material forming the basal bed of the succeeding Middle Ordovician formation.
The detrital chert forming the conglomerate bed represents reworked chert that accumulated on the weathered surface of the Knox Group after it was elevated above sea level and subjected to erosion, prior to resubmergence and deposition of the younger formations. This conglomerate is correlative with the Attalla Conglomerate which is widespread in Alabama (Butts, 1926, p. 121) and also well-developed ln southern Chattooga County, northwest Georgia. The Attalla Conglomerate also occurs in western Floyd County where in one place it is thick enough to be shown on the accompanying geologic map, figure 4, thus herein, is given formational rank in Georgia.
Ordovician strata also crop out in Furnace Valley in northernmost Floyd County, but the formations present there were not determined.
Hydrology.-This part of the Ordovician section probably will be of little use as an aquifer in most areas because it underlies steep, deeply dissected slopes. The steep slopes cause a rapid runoff and correspondingly low recharge; the deep dissection results in rapid loss of water through leakage.
Red and yellow mudrock and some sandstone appear at the surface in relatively flat-lying areas west and north of Heath Mountain and in Furnace Valley. Wells in depressions there can be expected to supply 2 to 10 gpm, depending on the amount of sandstone present. The water will be soft to moderately hard and may be high in iron.

Silurian System
Red Mountain Formation
The Red Mountain Formation of Silurian age was named by Smith (1876) for developments on Red Mountain east of Birmingham, Ala. The formation is an important source of iron ore in Alabama and has been worked on a moderate scale in Georgia.
Lithology.-The Red Mountain is composed of sandstone, shale and conglomerate. The base of the formation consists of about 100 feet of mediumgray coarse-grained sandstone, quartzite, and quartz-pebble conglomerate. Grains in the sandstone and quartzite are medium to very coarse, subrounded and subangular, and are fairly well sorted. The conglomerate is composed of wellrounded pebbles as much as 0.6 inch in diameter thinly scattered, but locally concentrated, in a matrix of medium and coarse-grained sand. Some layers of conglomerate contain pebbles of limonite or clay as much as 0.8 inch across, which weather out leaving smooth-sided hollows in the rock surface. Bedding in the basal unit is massive, generally ranging between 4 and 6 feet thick.
The middle part of the formation is composed of sandstone and shale in approximately equal proportions. The sandstone is medium to coarse grained, brown weathering, and most is in layers 2 to 4 feet thick. The sandstone layers which weather to a rusty brown are separated by varying thicknesses of dark-gray clay and silt shale that weathers to olive green or tan.
In tlie top 300 feet to 400 feet of the formation, the sandstone is mainly very fine to fine grained and occurs in beds from a few inches to about 2 feet thick. The sandstone beds are separated by varying thicknesses of shale.
The changing character of the Red Mountain from bottom to top is well displayed on the crest of Turkey Mountain. The top of the formation and its contact with the Armuchee Chert occur near the south end of the mountain; the basal conglomerate crops out a short way from the north end.
Distribution and thickness.-In Floyd County, the Red Mountain Formation is between 600 and 1,200 feet thick. Because it is very resistant to erosion, it upholds the highest ridges in the county.

34

including Horseleg, Turkey, Johns, Lavender, Turnip, Simms, and Heath Mountains.
Partial sections of the Red Mountain can be seen beside the Central of Georgia Railway at the west end of Lavender Mountain, along the road over Lavender Mountain about a mile northeast of Lavender Station, and beside the roads ascending and on top of Horseleg Mountain. The basal quartzite unit of the formation crops out in the cut of Georgia Highway 20 at the east end of Heath Mountain.
So far as the writer is aware, the Red Mountain does not crop out south or southeast of the Rome Fault. Spencer (1893, p. 86) identified the sandstone and quartzite on the ridges southwest of Cedartown, Polk County, as Red Mountain but these rocks intertongue with chert and without much doubt belong to the Frog Mountain Sandstone.
With the possible exception of the 3 or 4 feet of quartzite immediately above the Rockmart Slate at Elders Lake (described under Frog Mountain Sandstone) no indication of the Red Mountain was found in Polk County.
Hydrology.-So far as was learned, the Red Mountain is not used as an aquifer in the report area. Its outcrops are so high and remote that only Horseleg Mountain, which is conveniently close to Rome, is inhabited; the homes there are supplied water by a private distribution system.
Studies of the Red Mountain in other counties of the state show that in flat areas near a stream, or on gentle slopes near the base of a ridge, wells can be expected to yield between 2 and 10 gpm. In a few places where recharge is constantly available such as beside a stream that crosses the formation, a well may supply between 5 and 20 gpm. Such conditions exist in Floyd County where Cabin Smith Creek crosses the formation between Turnip and Lavender Mountains and in a few places along the south slope of Lavender Mountain, mainly near the northeast end. It may be possible to obtain a satisfactory supply in a few places on the southeast flank of Horseleg Mountain. In general though, the availablilty of ground water in the Red Mountain seems to be low. This is because most of the ridges upheld by the Red Mountain in Floyd County are

high, narrow crested, and steep sided and are formed by strata inclined from 30 to 90 degrees. As these conditions do not favor recharge or storage, the occurrence of an adequate and dependable supply of ground water in the formation will be rare, and the chance of obtaining a domestic well on the summit of most of the ridges is very poor.
One exception to this is Lavender Mountain which, because it is an anticline, for most of its length has a relatively broad crest that is underlain by nearly horizontal strata. Because of its breadth, the ridge is covered by fairly deep soil and this, coupled with the nearly flat bedrock should provide adequate recharge and storage, so that wells drilled in flat, low areas should supply between 2 and 10 gpm.
Water from the Red Mountain generally is soft, but it commonly has an objectionably high iron content. The concentration of iron in some of the water is so high that filtration is needed to make it potable and keep it from ruining porcelain fixtures.
In the past 3 years a need has arisen for ground water supplies in the Red Mountain Formation on Horseleg Mountain; people want to build homes on the northwest limb of the mountain, but the area is beyond the reach of the private distribution system. Wells are the suitable source of water and the Survey, in cooperation with the Georgia Department of Mines, Mining and Geology, has been called in to aid in selecting well sites.
Unfortunately, along this limb of the mountain, water seems to be in very short supply. The underlying rocks are steeply inclined to the northwest and because of this, the ridge generally is only 100 to 300 feet wide and slopes off abruptly to the east and west. Due to the narrowness of the ridge, erosion has kept soil accumulation to a minimum and the lack of an absorptive soil cover results in high runoff, so that little water finds its way into the bedrock. Furthermore, water reaching the bedrock is lost rapidly through leakage down the slanting bedding planes. It is this combination of low rate of recharge and rapid loss of water from storage that severely limits the quantity of ground water available in the Red Mountain along this part

35

of Horseleg Mountain.
It may be possible to develop a satisfactory home supply at a few places along the ridge where undulations in the structure have left relatively low dipping strata. Where the dips are gentler the ridge crest tends to be broader and have a thicker soil cover that is conducive to recharge. The most favorable conditions for finding water exist where a 1ocal drainage has cut a depression in a broad part of the ridge crest toward which ground water will migrate from at least two directions. A well positioned in the lower part of such a drainage probably stands some chance of tapping a yearround supply.
Devonian System
Frog Mountain Sandstone
The Frog Mountain Sandstone of Devonian age was named by Hayes (1894, p. 470) for Frog Mountain, Cherokee County, Ala. There the formation is about 300 feet thick and consists of fine- to coarse-grained red-weathering sandstone in the upper part, and sandy calcareous and cherty beds and dolomitic limestone in the lower part. In Alabama, the Frog Mountain has yielded many fossils of Middle Devonian (Onondaga) age (Butts, 1926, p. 157).
Lithology and thickness.-The Frog Mountain Sandstone appears to be a clastic facies of the Armuchee Chert; the two formations commonly intertongue and the Frog Mountain in many places includes beds and nodules of chert. In the report area the Frog Mountain is approaching its northeastern and eastern limits and therefore is very thin. In much of Floyd County it is present only as a thin layer within the Armuchee Chert.
The Frog Mountain in Floyd County varies from about 5 to as much as 25 feet thick and is made up of light- to medium-gray, fine- to medium-grained sandstone and vitreous quartzite that contain a high percentage of granular feldspar. The quartz grains are subrounded and subangular and commonly are frosted. Upon weathering, the rock becomes reddish brown and is speckled by rustcolored hollows formerly filled with feldspar.

Locally the Frog Mountain is highly ferruginous and its outcrops have been extensively prospected for iron.
In Polk County, outcrops of the Frog Mountain are scattered over a wide area south and southwest of Cedartown, but good exposures occur only in a few places. One is in the cut of the lower dam of Elders Lake. The Frog Mountain there is as much as 15 feet thick and consists mainly of light- to medium-gray, fine-grained feldspathic quartzite containing scattered quartz pebbles as much as a quarter of an inch in diameter. The quartzite weathers to light brown or medium dark brown. The upper 2 or 3 feet of the formation are lightgray to dark-gray quartzite that is outstandingly
different from that below, because its weathered surfaces are white and vitreous. In this exposure, the Frog Mountain rests unconformably on the Rockmart Slate and is overlain by the Fort Payne Chert, but faulting has repeated the sequence three times and the formation has a different thickness in each fault slice.
On the ridges around Elders Lake and in the valley immediately southeast of the lower dam, the Frog Mountain consists of light- to medium-gra)J fine- to coarse-grained quartzite. Most of the rock has a rounded nearly white vitreous surface, similar to the upper quartzite at the dam, and is unusually hard and flinty like the quartzite on and near Indian Mountain. The nearly white surface of the quartzite is separated from the darker interior by a rusty-brown or reddish-brown layer 0.1 inch to 0.25 inch thick. Bedding ranges from about 1 inch thick, chiefly in the lower part, to several feet thick near the top of the Frog Mountain. The lower thinner bedded layers tend to be less vitreous and softer than the more massive upper layers. Small quantities of thinly bedded chert are intercalated with the quartzite, particularly on the ridges north and east of Elders Lake and at one place, the quartzite is separated from the Rockmart Slate by about 10 feet of very dark gray chert containing abundant molds of crinoid stems. The presence of this chert in and beneath this quartzite was the principal reason for correlating the quartzite with the Frog Mountain rather than with the Red Mountain Formation, as was done by Spencer (1893, p. 86).

36

About a mile southwest of Elders Lake, in the cut made for the dam of Cupps Pond, the exposed Frog Mountain is composed of a lower 2.5-foot layer of quartzite, which rests on the Rockmart Slate, and an upper 1-foot layer of quartzite, separated by 2.5 feet of olive-green to very dark gray sandy, cherty material containing poorly preserved cup corals. The quartzite is fine to very coarse grained, highly ferruginous, and contains scattered quartz pebbles about 0.2 inch in diameter. Preserved on the rusty-brown surface of the weathered quartzite are faint impressions of cup corals and very large (3-inch) brachiopods and pelecypods. The thickness of the quartzite exposed in the cut changes abruptly. Within the cut of the dam the quartzite layers change in thickness abruptly, largely as a result of folding and duplication by faulting, and in the spillway the section is repeated several times.
From Cupps Pond westward toward Esom Hill the Frog Mountain increases in coarseness and becomes interbedded with, and in places overlies, a few feet of thinly to thickly bedded chert (Armuchee). West of Esom Hill, though, the chert disappears and is replaced by dark-gray to nearly black shale and slate that is unique in the area because it weathers to a very light gray. About a mile west of the state line in Alabama, the amount of shale increases and locally it is more abundant than the quartzite but farther west and northwest the quartzite again predominates and the shale is confined mainly to the lower part of the formation.
The other outcrop area of the Frog Mountain in Polk County is at Etna and Oremont. Immediately east and north of Oremont the formation consists of 20 to 30 feet of light-gray to dark-gray, brownweathering quartzite and sandstone containing granular feldspar. Chert layers and nodules occur sparingly throughout much of the rock as do poorly preserved gastropods, crinoid stem plates, and various fossil debris.
In the mine on the side of the ridge, about a quarter of a mile southeast of Oremont, the Rockmart Slate is absent and the Frog Mountain rests unconformably on the Newala Limestone. Pieces of dolomite from the Newala, along with chert

nodules, possibly from the same source, are incorporated in the basal quartzite layers of the Frog Mountain.
About half a mile southwest of Oremont, the Frog Mountain attains a thickness of perhaps 100 feet and forms a sizable ridge. There the formation consists of fine- to coarse-grained vitreous quartzite that on exposed surfaces has a nearly white chert-like surface similar to the quartzite on the ridge near Elders Lake. Quartz pebbles as much as 0.25 inch across occur in some layers. The interior of the rock is light gray to pink where slightly weathered and is flecked with cream-colored feldspar grains. Further weathering softens the rock and changes it to a rusty brown. As can be seen in nearby mines, the Frog Mountain at this location overlies at least 25 feet of Armuchee Chert and perhaps as much as 20 feet of Rockmart Slate.
About a mile west-southwest of Oremont massive light-gray quartzite of the Frog Mountain caps a narrow ridge where it overlies a thin section of the Armuchee Chert (formerly mistaken for chert of the Knox Group) and, where that is absent, rests on the Rockmart Slate.
Farther west on Etna Mountain and on Indian Mountain, the formation has increased in coarseness and much of the sandstone and quartzite are conglomeratic. Its thickness was not determined, but on Etna Mountain it probably is between 200 and 300 feet, and on Indian Mountain it is much thicker.
Distribution.-In Floyd County, the Frog Mountain is limited to a layer of quartzite 5 to 20 feet thick contained within the Armuchee Chert. It is exposed in the cut of the paved road that goes up the northeast end of Horseleg Mountain and in the cut of the Central of Georgia Railway at the southwest end of Lavender Mountain. The formation also crops out at several places along the east slope of Turkey Mountain, where it is highly ferruginous and has been extensively prospected for iron.
In Polk County, the Frog Mountain occurs in several widely separated areas. It is present on the crests and slopes of several ridges in the vicinity

37

of Elders Lake and extends from there to the ridges southwest of Cedartown., The formation makes up a prominent ridge west and southwest of Oremont, and is exposed in the mines east and north of Oremont. It crops out locally on the slopes of the hills of the Knox Group east and south of Oremont and Etna. As best as could be determined, the Frog Mountain makes up the lower part of Indian Mountain.
Fauna and correlation.-Although fossils are rare in the Frog Mountain, enough were found to clearly establish that the formation is younger than Early Ordovician, and in view of its stratigraphic relations, there is littie doubt that it is of Devonian age.
Weathered Frog Mountain in the spillway of Cupps Pond contains faint impressions of solitary corals and 3-inch brachiopods and pelecypods. Cherty material in the cut of the dam also contains poorly preserved solitary corals, some of them revealing internal structures.
From weathered sandstone of the Frog Mountain in the mine half a mile north of Oremont, Yochelson and Cressler collected a spiriferoid brachiopod that, although it was generically indeterminate, clearly is of post-Ordovician age. Some molds, possibly of pelmatozoan debris, also were present in the rock containing the brachiopod. In the same mine, other sandstone and quartzite of the formation display faint impressions of gastropods and very small crinoid stem plates.
As these were the only places fossils were found, mapping the Frog Mountain in isolated areas around Indian Mountain in Polk County and adjacent Alabama was done solely on the basis of lithologic correlation and stratigraphic position. For this reason, the identification of the rock on the south slopes of Indian Mountain should be considered tentative, until further work can be done to locate some fossils.
From Cupps Pond, where it is fossiliferous, the Frog Mountain forms a nearly continuous ridge that crosses into Alabama and swings northwestward and finally northeastward to re-enter Georgia near Etna. The formation is especially interesting in this part of Alabama because it develops an unusual character. For example, on Wheeler Hill, Cle-

burne County, and Baker Hill, Cherokee County, Ala., the Frog Mountain includes a large amount of extremely well-sorted quartzite and sandstone that is unlike anything present in other formations in the area. The rock is composed either of light-gray or of dark-gray quartz grains, depending on the location, that are well rounded, spherical, and frosted. Approximately 75 percent of the grains are in the 1-2 mm grade size (Crawford, 1957, p. 42). Most of the rock is cemented by quartz, but some layers have a matrix of light-gray-weathering, dark-gray clay. The coarser grained quartzite is so distinctive that it locally is known as "birdshot conglomerate" or "frogs-egg conglomerate" (Crawford, oral communication, 1965).
Rock composed of such highly sorted spherical grains is unique in the area and, therefore, is a valuable aid in correlating the Frog Mountain in the absence of fossils. It 'llso is helpful in distinguishing the Frog Mountain from Weisner Quartzite; according to John Rodgers (oral communication, 1964), who saw it in the cut of Alabama Highway 74 about a mile west of the Georgia line, this type of rock does not occur in the Weisner Quartzite. The Weisner is the only formation in the area that contains quartzite easily confused with that in the Frog Mountain.
From Baker Hill the Frog Mountain, including nun1erous layers of "birdshot conglomerate" and a lower section of light-gray-weathering shale, extends northward to an unnamed ridge south of the abandoned mining town of Bluffton and on to Bluffton Mountain. From there it swings eastward, part of the outcrop crossing a broad valley and extending up on the south slope of Indian Mountain, and the remainder continuing into Georgia where it makes up Etna Mountain and some lesser ridges at Oremont.
Where it makes the swing from Esom Hill into Alabama, and back into Polk County at Etna, the Frog Mountain crops out around the nose of a large anticline in the Knox Group. The Frog Mountain is in normal sequence from the Knox up through the Newala Limestone and the Rockmart Slate, and so far as exposures reveal, the sequence remains normal to the south base of
Indian Mountain. As Crawford determined (1957), Indian Mountain is a faulted synclinorium, and the strata on the south slope of the mountain are stratigraphically above the formations in the valley, rather than below them as formerly was supposed (Hayes, 1902).

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Hydrology.-No hydrologic data were available for the Frog Mountain Sandstone as its outcrops are uninhabited. But, judging by other largely sandstone aquifers, the formation can be expected to supply as much as 20 gpm to wells. The amount of water available will depend largely on the formation's thickness and the attitude of its beds.
In Floyd County, and in Polk County from Elders Lake to Esom Hill, where the Frog Mountain averages less than 20 feet thick, wells in Jow areas favorable for recharge probably will supply between 2 and 10 gpm. The formation is steeply inclined over most areas though, and will be beyond the practical reach of wells except in a narrow belt paralleling its outcrop. An exception to this occursnear Cupps Pond where the bedding has a low dip and the formation probably lies at a shallow depth over a wide area.
Between Cupps Pond and Esom Hill, the formation includes considerable bedded chert which may increase the availability of water. South of Esom Hill, the Frog Mountain is faulted over by the Rockmart Slate which may act as a confining layer to produce artesian conditions.
Near Oremont, the thickness of the formation increases to as much as 100 feet. In the thicker parts wells on gentle slopes probably will yield 5 to 20 gpm. The rock dips at a shallow angle beneath the valley and should provide a good source of water over a wide area.
On Indian Mountain large quantities of ground water may be available where deeply intrenched stream valleys cross the outcrop. The rock receives nearly constant recharge from surface water and ground water traveling down gradient along the stream courses, and should be capable of meeting large withdrawals by wells. Yields of 50 gpm or more may be possible. The wells would have to be positioned far enough upstream to be above a thick section of sandstone.
Water from the Frog Mountain probably will be soft, but it will tend to have a moderate to high iron content.
No springs of appreciable size are known in the Frog Mountain. A few very small springs seep from the base of Indian Mountain and at least one is used for a stock supply.

Armuchee Chert
The Armuchee Chert of Early and Middle Devonian age was named by Hayes (1902, p. 3) for exposures near Armuchee, Floyd County, Ga. The type section presumably is along and near Armuchee Creek where it crosses the end of Lavender Mountain.
Lithology.-The Armuchee is composed chiefly of medium to dark-gray chert that locally is sandy and ferruginous. In most weathered exposures it is light gray and where newly uncovered, it may have a rusty or reddish-brown surface. The chert normally is thin bedded although thick to massive beds generally occur, and in a few places the highly weathered chert largely is nodular. It is not unusual for the formation to contain scattered layers of ferruginous sandstone or very sandy chert which may or may not be feldspathic.
In Floyd County the middle and upper parts of the Armuchee commonly include a 5- to 25-foot unit of sandstone and quartzite that represents a northeastward extending tongue of the Frog Mountain Sandstone, a clastic counterpart of the Armuchee.
Distribution.-The Armuchee forms hogbacks along one or both flanks of the higher ridges of Red Mountain Formation and blankets the ends of the ridges that are anticlinal. Partial sections of the formation are exposed along the hogbacks where they are deeply dissected bylocal drainages. Better and more accessible outcrops occur along the paved road that crosses the northeast end of Lavender Mountain, three-quarters of a mile southwest of Armuchee; and along the Central of Georgia Railway at the opposite end of that mountain. The chert also crops out along the roads that ascend the northeast end of Horseleg Mountain and recently it has been uncovered in excavations made on the Shorter College campus in Rome.
Ten or more feet of the uppermost Armuchee are exposed in the cut of the paved road that crosses the south end of Turkey Mountain. Highly weathered Armuchee can be seen in the road metal pits on the west flank of Turkey Mountain near the north end, and steeply dipping layers of the formation, showing the massive character of the chert where it has weathered above ground, crop out on the hogback several hundred feet south of the road metal pits. On the east slope of Turkey Mountain,

39

about midway between the north and south ends, the upper part of the Armuchee is exposed, along with the Chattanooga Shale and a thin section of Fort Payne Chert; here, the top few feet of the Armuchee are medium to coarse-grained sandstone containing an abundance of feldspar grains.
In Polk County, the Armuchee crops out on several ridges around Elders Lake and along the ridge that runs between Cupps Pond and Esom Hill. A 20-foot section of the formation is exposed in the mine about half a mile southwest of Oremont. Weathered chert of the Armuchee is scattered in abundance along the ridge half a mile west and northwest of Oremont.
Thickness.-As best as could be determined from incomplete exposures, in northern Floyd County, the Armuchee varies from about 100 to 150 feet thick and in the central part of the county it seems to range between 50 and 100 feet thick. The formation thins to the southwest .and in Polk County it is only about 5 feet thick east of Elders Lake and perhaps as much as 30 feet thick on the ridge half a mile west of Oremont.

County, Tenn. The Maury is designated a member of the Chattanooga in the area of this report.
Lithology and thickness.-In Georgia, the Chattanooga consists of as much as 40 feet of black highly fissile clay and silt shale, locally containing thin layers of siltstone and fine-grained sandstone. The Chattanooga gradually thins toward the south and in Floyd County it has a thickness of about 10 feet. Upon exposure, the shale slowly changes from black to brown and finally becomes purplish brown or tan; in highly weathered slate its appearance is similar to that of long-exposed Lavender Shale Member of the Fort Payne Chert.
Maury Member
The Maury Member, lying at the top of the Chattanooga, is a 2- to 3-foot layer of greenish glauconitic shale or clay. The Maury contains phosphatic nodules one-fourth inch to 6 inches in diameter, and as nodules of this type do not occur in other formations, they enable identification of the Maury where stratigraphic sequence is indeterminate.

Utilization.-The Armuchee is an important source of road metal. Large tonnages of chert have been taken from pits on the west slope of Turkey Mountain.
The highly ferruginous sandstone at the top of the Armuchee on the east slope of Turkey Mountain has been prospected for iron but no commercial deposits were found.
Hydrology.-No wells were found that derive water solely from the Armuchee Chert. The Armuchee does, however, supply water to a high percentage of the wells that begin in the overlying Fort Payne Chert. The latter is so thin that wells pass through it and obtain water from both formations. For this reason, and because the formations are similar lithologically, the hydrologic properties of the Armuchee are discussed in the section of this report dealing with the Fort Payne Chert.
Chattanooga Shale
The Chattanooga Shale of Devonian and Mississippian age was named by Hayes (1891, p. 143) for exposures at Chattanooga, Tenn. The Maury Member of the Chattanooga Shale is of Early Mississippian age and was named for Maury

In Floyd County the Maury is invariably at the top of the Chattanooga and thereby provides a valuable top and bottom criterion. In places such as the road intersection about 0.75 mile west of Armuchee, exposures are so poor that the attitude of the Chattanooga would be in doubt were it not for the Maury indicating the top.
Distribution.-The Chattanooga and the Maury have a line of outcrop along the dip slopes of all the ridges of Red Mountain Formation and they can be observed in the deeper drainage courses there: they are well displayed on the east flank of Turkey Mountain. Other exposures occur beside the road that runs along Armuchee Creek near the northeast end of Lavender Mountain; and along the roads ascending the northeast end of Horseleg Mountain. A good exposure of the Chattanooga is in the cut of Georgia Highway 20, at the south end of Turnip Mountain. Phosphatic nodules in the Maury are well developed in the southeast comer of the road intersection at the south end of Turkey Mountain.
Neither the Chattanooga nor the Maury has been recognized in Polk County and apparently they were not deposited there.

40

Hydrology.-The Chattanooga Shale is not an aquifer because it is thin and has very low permeability. It does, however, affect local ground-water conditions.
In parts of Floyd County where the Lavender Shale Member of the Fort Payne Chert is absent, the Chattanooga may act as a confining layer above the Armuchee Chert, producing artesian conditions. But more importantly, the Chattanooga contains sulfides; ground water that comes into contact with it generally becomes charged with iron and hydrogen sulfide. In addition, the shale contains small concentrations of uranium which may be picked up by the water. For these reasons, wells penetrating the Chattanooga either should be properly cased to a depth below the shale, or if they derive water from above and below, have the shale effectively cased off. Otherwise, good quality ground water from the Fort Payne Chert or the Armuchee Chert may be sufficiently mineralized to render the entire supply unfit for use.
Mississippian System

product of highly siliceous carbonate. At any rate, on the west brow of Pigeon Mountain, Walker County, the only place where fresh exposures of the formation occur, the Fort Payne is thickly to massively bedded carbonate so siliceous that upon leaching it is reduced to thinly bedded chert without appreciable decrease in volume. East of Pigeon Mountain the formation undergoes a facies change, grading laterally into and becoming intertongued with calcareous shale and argillaceous limestone which Butts and Gildersleeve (1948, p. 44) named the Lavender Shale Member of the Fort Payne Chert.
In Floyd County where the Lavender Shale Member is well developed, the Fort Payne varies from as little as 10 feet to as much as 125 feet in thickness and is composed of light-gray to darkgray chert in layers ranging from less than 1 inch to more than 2 feet thick. The chert beds are very even and extend for hundreds of feet without noticeable variation. Individual layers are separated by irregular bedding surfaces, commonly marked by very thin accumulations of silt and clay.

Fort Payne Chert
The Fort Payne Chert of Early Mississippian age was named by Smith (1890, p. 11;)5-156) for development at Fort Payne, DeKalb County, Ala.
Stratigraphy.-The stratigraphic position of the eastward and southeastward extending tongues of Fort Payne Chert within Floyd County varies markedly with the location. At the south end of Turnip Mountain and the northeast end of Horseleg Mountain, for example, a thin section of Fort Payne immediately overlies the Chattanooga Shale. In north ,central Floyd County, on the other hand, the Fort Payne is separated from the Chattanooga by a considerable thickness of the Lavender Shale Member of the Fort Payne Chert. Large variations in position also take place within relatively short distances; on the east flank of Turkey Mountain, the Fort Payne succeeds the Chattanooga, whereas about a mile away, near the south end of the mountain, the Fort Payne lies more than 100 feet above the Chattanooga, at the top of the Lavender Shale Member of the Fort Payne Chert.
Lithology and thickness.-In all but the southernmost outcrops, the Fort Payne in Georgia consists of as much as 200 feet of thin- and thickbedded chert, which seems to be the weathering

In Polk County, the Fort Payne assumes a varied character. In western outcrops it is largely bedded chert similar to that in Floyd County, mixed with silty, argillaceous, somewhat fissile, material like the Lavender Shale Member. Farther east the proportion of silty and argillaceous material increases and east of Rockmart, siltstone, :fme-grained sandstone, and very silty and clayey chert form a major part of the Fort Payne. Indeed, much of the rock on the east side of the county that was mapped as Fort Payne wol!ld, have been shown as Lavender had delineation been practical under the circumstances. It was decided for the sake of simplicity to map all of this rock as a single formation, because it is a continuous unit overlying the Rockmart Slate.
On the east side of the county nearly all of the chert in the formation is recrystallized, and the sandstone and siltstone grains commonly exhibit secondary growth. The rock there is light to medium gray, very hard, and has a vitreous surface. It tends to form rounded boulder-like chunks 2 to 6 feet across, and in places these are scattered about in abundance.
Along the extreme southeast edge of the outcrop, where intense pressure was brought to bear by the Cartersville Fault, the formation is brec-

41

ciated. The breccia is made up of hard, angular pieces of light- to medium-gray recrystallized chert and siltstone mixed with softer, generally smaller and more rounded red, white, and tan pieces of similar material, all cemented into a mass by silica or iron oxide. Boulder-like chunks of breccia litter the ground surface and in many respects, the terrain resembles that underlain by the Attalla Conglomerate at the top of the Knox Group.
The silica cement, and in some places the iron oxide cement as well, is the most resistant part of the breccia, and as weathering progresses the rock surface becomes crisscrossed by silica and iron oxide protrusions that resemble box works. Where the iron oxide accumulates in unusual abundance, prospect pits have been opened, but no workable ore bodies have been uncovered.
On the ridge that extends north and northeast from the Seaborad Coast Line Railroad about 2 miles southeast of Van Wert, the basal Fort Payne either includes or overlies-exposures were too poor to be certain which-several feet of thinly bedded sandstone and quartzite that resembles the Frog Mountain Sandstone, as well as some of the sandstone in the Rockmart Slate. As its age could not be determined, the quartzite was mapped in the clastic unit of the Rockmart Slate. Further investigation may prove this quartzite to be Frog Mountain, or conceivably Red Mountain Formation.
Distribution.-The Fort Payne follows a line of outcrop along the dip slopes of all the ridges of the Red Mountain Formation in Floyd County, and is exposed at innumerable places throughout this distance. Probably the best single exposure of the formation is in the cut of U. S. Highway 27 at Crystal Springs. Highly weathered Fort Payne can be seen in the cut of the same highway 1 mile south of Armuchee. The basal Fort Payne is in contact with the Chattanooga Shale where Georgia Highway 20 cuts across the south end of Turnip Mountain.
In Polk County the Fort Payne occupies a broad area east of Aragon, caps a few ridges near Rockmarl, and crops out along several narrow faulted ridges south and southwest of Cedartown. One of the best exposures of the formation is in the road metal pits beside Georgia Highway 100, half a mile south of the intersection with U.S. Highway 27.

Fauna and correlation.-In a few localities, the Fort Payne is moderately fossiliferous. Crinoid stem plates as much as an inch in diameter occur along with horn corals, brachiopods, pelecypods, and bryozoa. More typically, though, the formation contains few fossils. If any are present, they are apt to be crinoid stem plate . Even so, these can be diagnostic and are especially helpful in distinguishing the Fort Payne from the Armuchee Chert where exposures are poor and other criteria are wanting. According to Butts (1926, pp. 166, 167) and Butts and Gildersleeve (1948, p. 45), crinoid stems half an inch or more in diameter are common to the Fort Payne of Alabama and Kentucky, and are an infallible criterion for distinguishing the Fort Payne from older formations.
In Polk County, fossils have been found in several places. One locality having abundant specimens is the road metal pits on either side of Georgia Highway 100, half a mile south of the intersection with U. S. Highway 27. Fossils of Mississippian age were first reported from these pits by Butts and Gildersleeve (1948, p. 53), who found Platycrinus and a fragment of Spirifer(see plate 2, fig. 9). Butts did not recognize the chert as Fort Payne, however, but thought it was part of the Rockmart Slate and thereupon mistakenly dated the Rockmart as Mississippian (fig. 10).
Nearly all of the rock in the road metal pits is fossiliferous, but that in the pit east of the road is less weathered and the fossils there are better, though generally not well preserved. Fossils collected from the pit east of the road and identified by J. T. Dutro, Jr. (U.S.G.S. Colin. No. 21730-PC) include: abundant echinodermal debris, indeterminate; both large and small hor corals, generically indeterminate; tabulate corals, possibly Cladochonus; a large indeterminate spiriferoid that may be the same as Brachythyris of the next collection; Composita? sp.; and Torynifer cf. T. pseudolineata (Hall) (see plate 2).
Chert and siliceous material in the pit on the west side of Georgia Highway 100, 0. 7 mile south of the intersection with U. S. Highway 27 and about 0.2 mile south of the above pit (U.S.G.S. Colin. No. 21731-PC), according to J. T. Dutro, Jr., included indeterminate echinodermal debris; a generically indeterminate small horn coral; Leptogonia cf. L. analoga (Philips); Brachythris cf. B. suborbicularis (Hall); Spirifer sp., two species indeterminate; Tornyifer cf. T. pseudolineata (Hall); and Cleiothyridina? sp.

42

Figure 10. Steeply inclined Fort Payne Chert at top of Rockmart Slate. .

The cut of the same highway 0.1 mile farther south (U.S.G.S. Colln. No. 21733-PC) yielded echinodermal debris, indeterminate; and a trilobite pygidium, indeterminate.
Numerous fossils were found in dark gray siliceous shale (Lavender Shale Member) and highly impure chert and siltstone near the northeast end of the lower dam of Elders Lake (U.S.G.S. Colln. No. 21735-PC). The collection included echinodermal debris, a rhynchonelloid brachiopod, pectinacean pelecypods, muculacean pelecypods_, other pelecypods, low-spired gastropods, and pleurotomariacean gastropods, all indeterminate. According to John Pojeta, the pectinaceans indicate a Devonian or later Paleozoic age, but none of these specimens are characteristic Devonian types.
A collection from the north shore of the same lake, between 300 and 600 feet southwest of the dam, and at the same stratigraphic position (U.S.G.S. Colln. Nos. 21736-PC and 21737-PC) included echinodermal debris, Brachy thris sp., probably like that at U.S.G.S. 21731-PC, Cypricardella (or Cypricardinia ), Sinuitina? sp., and an indeterminate pleurotomariacean.

John Pojeta states that Cypricardella is known from Devonian and Mississippian age rocks and that the range of Cypricardinia is Silurian to Mississippian. Thus, these fossils are of little aid in correlating this chert with that on Georgia Highway 100. But, of the gastropods, Ellis L. Yochelson states, "Sinuitina is reported to range from Silurian to Permian, although it is known from only one locality each in the Pennsylvanian and Permian. Specimens occur in some abundance in the Coral Ridge Member of Conkin (1957) of the New Providence Formation in Kentucky. They were described by Conkin along with a form which he called Bembexia ellenae. That speCies is fairly elaborately ornamented and, in so far as this crushed pleurotomariacean material can be compared, they are similar." The New Providence Formation is of Osage age, thereby suggesting that the chert at Elders Lake is correlative with the Fort Payne, or at any rate the Lavender Shale Member, which much of the rock more closely resembles.
According to J. T. Dutro, Jr., the collections consisting of a brachiopod-coral-echinoderm assemblage are Mississippian in age, probably an Osage

43

equivalent. Other collections contain distinctive brachiopods that likewise suggest an Osage equiva- . lent. On this evidence, the formation is identified as Fort Payne Chert.
Tlte Fort Payne at several other localities in Polk County yields poorly preserved fossils of the same general types. A variety of specimens was seen in the road metal pit just east of the paved road on the ridge, half a mile south of Pine Bowers Church (U.S.G.S. Colin. No. 21732-PC) including Torynifer? sp. (see plate 2, fig. 13). Molds of crinoid stem plates abound in chert on the ridge south of Old Brewster School. Poorly preserved fossils of various types also are common in the Fort Payne and Lavender Shale Member about 2 miles southwest of the center of Rockmart. So far as is known, the httter locality is the southeasternmost occurrence of the fossils in the formation; east of there all faunal evidence seems to be absent, possibly having been obliterated by the combined effects of recrystallization, cleavage, and brecciation which everywhere affects the formation.
Hydrology.-The water-bearing character of the Fort Payne Chert and the Armuchee Chert are discussed together. This was done because the two formations are alike lithologically, and because wells beginning in the Fort Payne commonly pass through it into the Armuchee and derive water from both formations. Moreover, in west-central Floyd County, where the lower part of the Fort Payne is thickly developed, it is separated from the Armuchee only by the thin Chattanooga Shale, and for practical purposes the two chert formations constitute one hydrologic unit.
Although they presently are little used as aquifers, the Fort Payne and the Armuchee are important because they have large potential. They seem capable of supplying moderate to large yields to wells over much of their outcrop area. At the same time, however, due to the high permeability of the chert, both the Fort Payne and the Armuchee are easily contaminated and, consequently, they present special problems of well location and construction
Comparatively little hydrologic data could be obtained for the formations as they uphold ridge areas where few people reside. From what was learned it seems that everywhere except on steep slopes and on narrow ridge crests, the formations can be expected to yield between 5 and 50 gpm to

wells less than 150 feet deep. On fairly broad ridges such as the Beach Creek Anticline, supplies adequate for domestic needs probably can be obtained. Well 3JJ36, for example, which is 149 feet deep, was test pumped at the rate of 10 gpm; at the end of 3 hours and after it had drawn down only 7 feet, the water level stabilized at a depth of 77 feet below land surface. Even though this test was very limited, it gives a specific yield for the well of about 1.4 gallons per minute per foot of drawdown and indicates that it can supply considerably more than 10 gpm.
In the few places where the formations underlie valleys near a stream, such as at Crystal Springs and at Armuchee, yields of 50 to 100 gpm or more probably are possible. However, as water can travel far through the chert without being purified, caution must be exercised not to locate a well dangerously close to a stream.
The quality of the water from the Fort Payne and the Armuchee generally is good. The water is reported to be soft and it commonly is referred to as "freestone." The only problems of water quality probably originate in the Chattanooga Shale; wells penetrating the Chattanooga may be contaminated to a greater or lesser degree by sulfides and iron the amount of contamination depending on the thickness and the permeability of the shale at that place. This problem can be avoided by properly casing off the Chattanooga but, mainly for economic reasons, it is rarely done.
In Floyd County where the Armuchee and the Fort Payne make up hogbacks that parallel the high ridges of the Red Mountain Formation, the chert beds commonly are inclined from 20 to 45 degrees. Wells drilled near the base of a hogback may stand a good chance of tapping water under artesian pressure sufficient to result in a flowing well. Artesian conditions are most likely in the Armuchee as it is confined beneath the impervious Chattanooga Shale, but in the parts of Floyd County where the Fort Payne is succeeded by an appreciable thickness of the Lavender Shale Member, artesian conditions in it also may exist.
Several small springs discharge from the base of the ridges upheld by the formations, but the flows of all but a few are so small they are used only for stock watering and domestic supply. Spring 5KKS1, on the other hand, discharges about 0.2 mgd and furnishes water for the Girl Scouts of America camp.

44

The chert beds in the Armuchee and the Fort Payne are very even and continue uninterrupted for hundreds of feet, making it possible for ground water to move great distances along the bedding plane openings and through joints without undergoing filtration to remove impurities. For this reason, wells and springs in the formation are especially susceptible to pollution and contamination.
The danger of pollution was forcefully brought to public attention in the summer of 1963 by an epidemic that spread through the Girl Scouts of America camp in northern Floyd County. As health officials quickly determined, the infection was transmitted by the water supply which was being pumped, unchlorinated, from spring 5KKS1. The spring is topographically below and down dip from the main buildings of the camp.
Tests revealed that the bacteria reaching the spring originated in flush toilets that recently had been installed at the camp. Fluorescein (a dye) flushed down the toilets, to the consternation of everyone involved, appeared in the spring water in less than 48 hours. To reach the spring, the dye had to pass through the septic tank, seep from the field lines into the aquifer, and travel several hundred feet along the bedding planes. The short travel time resulted because the septic tank had been placed up hill from and almost directly on strike with the spring. Polluted water passed virtually unfiltered from the deeply buried field lines into the bedding plane openings of the chert and traveled rapidly down gradient to the spring.
Correcting this condition involved considerable expense; it was necessary to move the septic tank and the field lines down hill from the main camp far enough to insure that the effluent was topographically well below the spring.

the bedding, it is necessary to consider equally the topographic setting and the geologic structure in choosing a well site or disposing of waste.
Lavender Shale Member
The Lavender Shale Member of the Fort Payne Chert of Osage age was named by Butts and Gildersleeve (1948, p. 44) for exposures along the Central of Georgia Railway a third of a mile west of Lavender Station, Floyd County, Ga.
Hurst (1953, p. 218) showed that on very fresh exposures, much of the Lavender contains more than 50 percent lime; consequently, he suggested dropping the word "shale" from the name. However, in most natural exposures and in all but the deepest manmade ones, weathering has reduced the rock to calcareous mudrock or shale. Thus, the original name "Lavender Shale Member" is being retained because it is more descriptive of the formation as it normally appears at the mrface. The name Lavender Shale Member of the Fort Payne Chert as used in this report has been adopted by the U. S. Geological Survey.
Lithology.-At its type locality in Floyd County the Lavender Shale Member consists of massively bedded greenish mudstone and olive-gray shale containing abundant crinoid stem plates half an inch or more in diameter and several other types of fossils, notably bryozoa The formation also contains large geodes that are lined with crystals of calcite or quartz, or both.
The rock at the type locality is moderately to highly weathered and thus it is fairly typical of the formation as it generally appears at the surfac~. Relatively fresh Lavender, on the other hand, such as occurs in well cuttings, deep excavations, and some quarries, has a significantly different appearance.

This unfortunate event brings into focus the extreme importance of carefully locating well sites and of positioning any source of pollution or contamination, whether human or animal, sufficiently far from and adequately down gradient from a well or spring. In every instance, it is imperative that the gradient for both surface water and ground water be taken into account and that due consideration be given the dip and strike of the formations involved. With chert aquifers especially, as water readily moves along and at right angles to

Comparatively fresh Lavender Shale is exposed in the quarry on the east side of U.S. Highway 27, at the overpass of the Southern Railway in the northern part of Rome. It is mainly interbedded dark gray to nearly black, highly impure limestone, and calcareous claystone and siltstone. A few layers of noncalcareous siltstone also occur. Discontinuous chert layers and nodules rarely more than 2.5 inches thick are scattered throughout the section. The chert is dark gray and commonly is crisscrossed by fractures filled with calcium car-

45

bonate. Geodes as much as 6 inches in diameter, lined with quartz and calcite crystals, are fairly common.
Weathering of the Lavender takes place rapidly and blocks that were quarried 30 years ago have changed from dark gray to light, medium, or bluish gray, and ones longer exposed have become tan or tan with an orange cast. As the rock decomposes, it breaks down into small irregularly shaped pieces that have rough bedding surfaces; the more silty pieces are similar in appearance to the pieces of siltstone that collect in the residuum of the Floyd Shale. The chert in the Lavender changes from dark gray to tan and, with the solution of calcium carbonate from the fractures, it splits into small straight-sided pieces.
The geodes that occur in the Lavender are unique to it and to the Fort Payne Chert in Floyd County. Because of this, they are an important aid in identifying the weathered Lavender. The geodes range from about half an inch to more than 6 inches across, and all but the smallest, which are solid, are lined with dirty-white crystals of quartz or calcite, or both. Although these geodes are not present in all outcrops of the Lavender, they do occur in most and can play an important role in separating the Lavender from the Floyd Shale with which it may be in contact. Geodes were not found to occur in the formation in Polk County.
Massively bedded limestone cropping out in the Oostanaula River beneath the bridge at the north end of Turkey Mountain seems to be part of the Lavender as it is below the Fort Payne Chert that marks the top of the Lavender in the pit near the bridge. Its relative position indicates that the limestone lies above the highest shale of the Lavender exposed in the road cut, but its thickness could not be determined due to limited exposure.
South and southwest of Cedartown in Polk County, the Lavender Shale Member is mainly medium to light-gray or tan silty and cherty shale that intertongues with and is interbedded with the Fort Payne Chert. East of the Cedartown area, the Lavender generally is less silty and it remains a fairly thick unit nearly as far east as Rockmart, but does not seem to be present east of there.
Distribution.-Good exposures of the Lavender Shale Member in Floyd County can be seen along

the road that crosses the south end of Turkey Mountain for a distance of about a mile west of the Oostanaula River. Unusually fossiliferous Lavender was uncovered in the cut of Davis Road at the north end of Turkey Mountain. The formation is present at several places near Crystal Springs and beside U. S. Highway 27 south of Armuchee Creek. The freshest exposures of the Lavender in the study area are in the quarry and nearby railroad cuts on the east side of U. S. Highway 27 at the overpass of the Southern Railway in the northern part of Rome. Other good outcrops occur in the Oostanaula River just north of the Southern Railway bridge and near the intersection of Shorter Avenue and Horseleg Mountain Road in West Rome. Extensive outcrops are present west and southwest of the General Electric Plant where the Lavender makes up a slight elevation along the south edge of the Garden Lakes Subdivision. The formation is exposed beside Georgia Highway 20 just west of the crossing over the Southern Railway about 5 miles west of Rome.
The Lavender is present in most outcrops of the Fort Payne in Polk County west of Rockmart It is well exposed in the road metal pit east of Georgia Highway 100, half a mile south of the junction with U. S. Highway 27: and it crops out at the south end of the cut made for the lower dam of Elders Lake. A good outcrop of the shale occurs along and in the valley west of the unpaved road, just south of the intersection 1.8 miles southwest of the center of Rockmart.
Fauna and correlation.-The weathered Lavender Shale Member in Floyd County locally, although not commonly, yields crinoid stem plates 0.5 to 1.0 inch in diameter, along with solitary corals and a few trilobites.
The Lavender in western and central Polk County is moderately fossiliferous and large numbers of specimens were collected there. The fossils were used to establish the presence of the Fort Payne Chert in the county and therefore are listed and discussed in the section dealing with the Fort I>ayne. They show that the Lavender is an Osage equivalent.
Stratigraphic relation.-The Lavender Shale Member represents the eastern and southeastern clastic facies of the Fort Payne Chert. West of a line formed by Taylor Ridge and Whiteoak Mountain in Chattooga, Walker, and Catoosa Counties,

46

Ga., the Lavender Shale Member amounts to little more than a few thin shale layers between beds of chert or to a shale section 5 to 20 feet thick randomly positioned within the Fort Payne. East of there, however, the Lavender becomes a prominent member, replacing from 50 to 125 feet or more of the Fort Payne over wide areas. Moreover, in central Floyd County, where the Lavender reaches a maximum development, it replaces the entire section of Fort Payne except for 10 to 20 feet of chert at the top. The Lavender attains a thickness of about 200 feet near the town of Armuchee and near the south end of Turkey Mountain.
Hydrology.-Ground water in the Lavender Shale Member occurs mainly in joints. The formation has a well developed system of interconnected joints, but they are tight, so the availability of ground water is low.
Although the bulk of the Lavender contains more than 50 percent lime, the large proportion of insoluble material present effectively retards enlargement of joints by solution. Decalcification takes place along the joints, but it rarely penetrates the rock more than about a quarter of an inch. Further solution is prevented by a hard layer of insoluble residue that remains on the joint surface. Thus, the openings remain tight and the formation has small storage capacity. Moreover, the layers of fairly pure clay shale throughout the formation impede the vertical movement of water.
Only limited hydrologic data were available for the Lavender Shale Member, but as far as could be determined, wells in the massive mudstone and very impure limestone average less than 10 gpm. The water generally is soft to moderately hard and much of it contains noticeable quantities of iron. Iron rarely causes a serious problem, however.

dull, rather rough bedding surface. Layers of brown-weathering siltstone and fine-grained sandstone less than 2 inches thick commonly are interlayered with the shale. Clay shale that has a waxy surface is abundant locally, and north of judy Mountain it is mined for use in making brick.
Much of the shale in the Floyd is highly carbonaceous, and on fresh exposures it is very dark gray to nearly black, resembling the Chattanooga Shale. Weathering bleaches the shale to light gray, then alters it to light brown, chocolate brown, or purplish brown, and finally to pinkish purple. Limonite box works are abundant and remain in the soil after the shale has decomposed.
Small irregularly shaped pieces of purplishbrown sandstone and siltstone weather out of the shale and collect on the surface of the ground, giving it a distinctive purplish cast. Even in the absence of outcrops, the purplish soil that forms on the Floyd is distinctive enough to enable ready identification. Although the shale generally is unfossiliferous, the pieces of sandstone and siltstone in the soil commonly contain impressions of crinoid stems or other fossils.
The Floyd Shale generally is less fissile than the shale of other formations with which it comes in contact. The silty shale tends to split into large slabs about a quarter of an inch thick, whereas the shale of the Conasauga, for example, has a high degree of fissility and yields small flakes only a fraction as thick. Some weathered clay shale of tbe Floyd has a character similar to that of the Conasauga, but, except where extremely decomposed, normally contains sufficient carbon and mica to be distinguishable. In a few areas, however, as north of Rome, the weathered clay shale of the Floyd is almost identical to the shale of the Conasauga, so that fossils are required to make an accurate separation.

Floyd Shale
The Floyd Shale of Mississippian age was named by Hayes (1891, p. 143) for development in Floyd County, Ga. The formation is mainly dark-gray clay and silt shale, but includes a thick unit of limestone at the base and the Hartselle Sandstone Member near the top.
Lithology.-In Floyd County the formation consists mainly of silty micaceous shale that has a

The Floyd Shale includes a basal unit of limestone that crops out at several places in Floyd County and locally is extensively quarried. The unit is composed primarily of thickly to massively bedded medium-gray limestone, much of which is sufficiently- pure to be used in making cement. In the Ledbetter quarry in the north part of Rome and on the west side of the Beach Creek Anticline the unit has a thickness of about 300 feet, but in other areas it does not appear to be that thick. Moreover, the exposures of the limestone are so

47

few and so widely scattered, it is possible the unit greatly thins or pinches out between outcrops.
In Polk County, the character of the Floyd Shale differs greatly with the outcrop location. Beside Gem:gia Highway 100, about half a mile south of the junction with U. S. Highway 27, and a few yards south of the road metal pits, the Floyd is dark-gray greenish weathering slate and shale containing a few beds of fine- to medium-grained, brown-weathering sandstone, half an inch to more than 6 inches thick in which are presenied impressions of minute crinoid stem plates. The shale there is in normal stratigraphic position above the Fort Payne Chert. It apparently was misidentification of this outcrop as Rockmart Slate that led Butts and Gildersleeve (1948, p. 53) to date the Rockmart Slate incorrectly.
The Floyd Shale in this outcrop is in normal stratigraphic position above the Fort Payne Chert, but as can be seen along the south side of the ridge west of the road, it is faulted over by the sandstone, conglomerate, and slate of the Rockmart, which in turn is overthrust by two slices of folded Fort Payne Chert.
East of Van Wert, adjacent to the Cartersville Fault, the Fort Payne Chert is succeeded by darkgray to nearly black phyllite which tentatively has been identified as Floyd Shale on the basis of apparent superposition and character; the phyllite was derived from carbonaceous shale or slate similar to that forming the Floyd in other areas. Moreover, the phyllite is lithologically dissimilar to the metamorphic material across the Cartersville Fault and has a different attitude.

Floyd County. Hayes considered the Hartselle as marking the top of the Floyd Shale, but in Chattooga County, Ga., to the north, a considerable thickness of Floyd Shale succeeds it. For this reason, the Hartselle in Floyd County is considered a member of the Floyd Shale.
On Judy Mountain, the Hartselle Sandstone Member is about 300 feet thick and consists of light to medium gray, thinly to massively bedded, very fine--to medium-grained sandstone and quartzite. Siltstone and quartz-pebble conglomerate also make up an important part of the formation. Siltstone is especially common near the base.
In the vicinity of Rocky Mountain, the Hartselle ranges in thickness from about 50 feet to 200 feet. It is thin bedded, generally 6 inches to 1 foot thick, and is very fine to medium-grained sandstone and siltstone. The fresh rock is very light to light gray, and, like the rock on Judy Mountain, weathers to a rusty brown or maroon.
Distribution.-The Floyd Shale occupies large areas in northern and western Floyd County. It is exposed in numerous cuts along Georgia Highway 20 between Rome and the Alabama State line. A sandy facies of the Floyd crops out beside the spur of the Central of Georgia Railway west of Judy Mountain. Both silt and slay shale are well exposed along the paved road between Garden Lakes Subdivision in West Rome and Lavender Station. The fairly fresh shale in the road cut at Floyd Springs and along the road west of Rocky Mountain is nearly black and resembles the Chattanooga Shale.

In the large mine at Oremont, and in another 0.5 mile northeast of there, the Floyd Shale is dark gray, silty, and includes pyritic nodules that commonly contain well-preserved fossils. The shale weathers 1to tan and purplish brown. A few fine- to medium-grained sandstone layers as much as 6 inches thick occur in places.
Hartselle Sandstone Member
Sandstone at or near the top of the Floyd Shale was mapped by Hayes (1902) as the Oxmoor Sandstone, but that name has been discarded in favor of Hartselle, as restricted by Butts (1926, p. 193). The Hartselle makes up Judy Mountain and the prominent ridge encircling Rocky Mountain in

The sandstone at the top of the Floyd, the Hartselle Sandstone MemberJis displayed in the cut of the paved road that runs south out of Crystal Springs across Little Texas Valley where the road cuts through the low ridge upheld by the formation.
The basal limestone unit of the Floyd is well exposed in the Ledbetter quarry north of Battey State Hospital, in the abandoned quarry beside U. S. Highway 27 at the bridge over Dry Creek, and in the old quarry a short distance north of Russell Field. The limestone also crops out beside the unpaved road, just south of the bridge over Beach Creek, west of Horseleg Mountain, and along King Creek north of Early on the west side of the

48

county. A small outcrop can be seen in the Oostanaula River about 4 miles northeast of the center of Rome, and on the west bank of that river where it passes Turkey Mountain.

3 and 20 gpm; the largest reported yield was 22 gpm. Eighty inventoried wells in the Floyd had an average depth of 83 feet; the deepest well was 295 feet deep.

In Polk County, the Floyd Shale underlies a large part of the valley near Oremont. Isolated outcrops of Floyd lie above the Fort Payne Chert south and southwest of Cedartown. The very dark gray to nearly black phyllite believed to be Floyd
Shale is exposed near tJ. S. Highway 278 adjacent
to the Cartersville Fault east of Van Wert.
Fauna and correlation.-Fossils are fairly abundant in much of the Floyd Shale in Floyd County, and the age of the formation and its general correlation have long been established.
In Polk County, on the other hand, the Floyd Shale was not recognized prior to the work of Crawford (1957) and its age there had not been extablished. Crawford collected several fossils from pyritic nodules exposed in the iron mine 0.5 mile north-northeast of Oremont. Among these, he identified Lyrogoniatites newsomi georgiensis Miller and Furnish, a nautiloid cephalopod (Crawford, 1957, p. 48).
Cephalopods collected from the same locality (U.S.G.S. Colln. No. 22703-PC) by the writer (see plate 2, fig. 8) were identified by Mackenzie Gordon, Jr., as Goniatites cf. G. kentuckiensis Miller and Neoglyphioceras georgiensis (Miller and Furnish). These fossils indicate an age equivalent to early Chester for the Floyd Shale at this locality.
Thickness.-The total thickness of the Floyd Shale never has been accurately determined because exposures are intermittent and the shale is highly folded and faulted. Hayes (1902) measured a section between Simms and Lavender Mountains, arriving at a figure of 1,200 feet.
The thickness of the Floyd was not measured directly in Polk County because of poor exposures. Judging from the distance across the outcrop, however, the formation south of Cedartown is about 1000 feet thick, and in the Oremont area it probably is between 200 and 300 feet thick.
Hydrology.-Wells in nearly all areas of the Floyd Shale yield water in sufficient quantities to supply a home or farm. Most wells furnish between

The quality of the water in the Floyd varies from good to very poor. About 55 percent of the wells inventoried were reported to have water ranging from soft to very hard, but otherwise of good quality. The remaining 45 percent yield water containing bothersome quantities of iron. In nearly half of these wells the iron concentration is so great that the water rapidly stains porcelain fixtures, and precipitates to form sludge in toilet tanks. Filtration is needed to bring the water to acceptable standards.
Wells having high-iron water show definite patterns of occurrence Iron is common in wells penetrating the lower part of the Floyd; some of limestone unit, and, as they are reported to yield limestone unit and, as they are reported to yield hard water, probably are in the limestone. Others, though, have soft water and seem to be in shale. A group of these high-iron wells occurs near Arrowhead Lake in northern Floyd County; others are clustered around Turkey Mountain and two are northwest of Armuchee.
The occurrence of high-iron water also is common in wells that are close to the axes of the major synclines in the Floyd Shale. This occurrence probably is related to t'l.e structure because the wells obtain water from a wide range of stratigraphic positions. A string of these wells is located south of Everett Spring, some are present northwest of Armuchee, and others are east of Judy Mountain.
Wells in or close below the Hartselle Sandstone Member have a high incidence of iron water. The iron probably originates in the sandstone. Wells at this horizon are located along the road going from Armuchee to Little Texas Valley.
No clear relationship seems to exist between well depths and the prevalence of iron in the water. Nor is there any indication, except possibly at the base of the formation, that the presence or absence of lime in the water is related to the iron concentration.
A few springs discharge from the Floyd Shale. Most are small and are used only for stock

49

watering. One spring, 3JJS4, flows about 0.5 mgd. A sample of this water had a total hardness of 85 ppm and an iron content of 0.07 ppm. Spring 4KKS2 flows about 0.3 mgd and is unused.
Bangor Limestone
The Bangor Limestone of Mississippian age, named by Smith (1890, p. 155-157) for Bangor, Blount County, Ala., originally included all rocks of Mississippian age above the Fort Payne Chert. Butts (1926, p. 195) later restricted the Bangor to the limestone above the Hartselle Sandstone Member of the Floyd Shale and below the Pennington Shale. The restricted usage is followed in this report.
Lithology and thickness.-The formation in Floyd County consists of thickly to massively bedded, blue-gray to gray, very pure limestone. Some argillaceous limestone and calcareous shale underlie the Bangor. An undetermined thickness of shale, probably a thinned extension of the Pennington Shale, overlies it. The Bangor is about 300 feet thick.
Distribution.-The Bangor crops out on the slopes of Rocky Mountain about 8 miles northwest of Rome in Floyd County, and underlies the narrow valley between Rocky Mountain and the ridge of the Hartselle Sandstone Member of the Floyd Shale. The Bangor is not known to occur in Polk County.
Hydrology.-Qnly one well was inventoried in the Bangor Limestone; it is 70 feet deep and reportedly yields 8 gpm of hard water.
Information obtained from the Bangor in other areas of the state shows that the formation, in general, is an excellent aquifer in low-lying areas, but has moderate to low productivity on steep slopes.
On the gentle slopes at the base of Rocky Mountain, and in the comparatively flat lying parts of the adjacent valley, the Bangor can be expected to yield between 3 and 20 gpm. In favorable locations near sources of recharge, the yields may exceed 50 gpm. The water will be hard but generally low in iron content.

Pennsylvania System
The Pennsylvanian System is represented in Floyd County by about 350 feet of sandstone, conglomerate, and shale. Although no attempt was made to correlate them with formations established in other areas, the rocks in Floyd County include lithologies that closely correspond to units on Lookout Mountain, Walker County, Ga., that Johnson (1946) included in the Gizzard and Sewanee Members of the Lookout Sandstone. The Lookout Sandstone of Johnson is equivalent to the Gizzard Formation and Sewanee Member of the Crab Orchard Mountains Formation as designated by Culbertson (1963, p. 51).
Lithology, thickness and distribution.-The rocks of the Pennsylvanian System can be grouped into 3 main units.
The lower unit, which ranges between 50 and 75 feet thick, is predominantly medium- to coarsegrained, thin- and thick-bedded sandstone, but includes an undetermined thickness of dark tanweathering shale at the base. This unit is followed by a middle unit composed of about 100 feet of thin-bedded fine- to m'edium-grained sandstone interlayered with a little tan-weathering sandy shale. The upper unit consists of about 100 to 150 feet of coarse-grained thickly to massively bedded sandstone and beds of conglomerate containing well-rounded pebbles of white quartz.
The Pennsylvanian System crops out only on Rocky Mountain in Floyd County.
Hydrology.-At the time of this investigation, the rocks of Pennsylvanian age in Floyd County were not being used as an aquifer, and no hydrologic data for them were available. Information obtained from other parts of the state indicate, however, that in most places, wells less than 300 feet deep can be expected to yield between 2 and lO gpm and those favorably located may supply as much as 50 gpm. Near the edge of the outcrop, though, which ends in high cliffs, only dry wells are likely, as ground water rapidly drains out of the cliff faces.
Water from the wells will tend to be soft and have a moderate to high iron content. The iron content of some of the water may be so high that filtration will be .required to make the water potable.

50

Cambrian to Pennsylvanian Systems
Talladega Slate
The Talladega Slate was named by Smith (1888) for exposures in Talladega County, Ala. The best available evidence seems to indicate that the Talladega is composed of rocks ranging in age from Precambrian to Carboniferous. Butts (1926, p. 61) believed that the Talladega probably is composed of shoreward clastic deposits that accumulated at intervals during the entire Paleozoic Era.
Litholo~ and thickness.-In Georgia, the Talladega consists primarily of alternating zones of greenish-gray phyllite and dark gray to nearly black carbonaceous phyllite, much of which includes thin beds of quartzite and graywacke. In a few parts of the formation, quartzite and graywacke become the principal constituents, though phyllite rarely is wanting altogether.
Butts (1926, p. 58) estimated the thickness of the Talladega in Alabama to be about 30,000 feet.
Distribution.-The Talladega underlies all of Polk County south and east of the Cartersville Fault. The Talladega in Polk County is the north-ern part of a broad belt of the formation that extends from the Cartersville Fault southward across Haralson County.

followed into the area of the lower part of the type Talladega.
The other unit of the Talladega traced was a layer of fairly pure quartzite that makes up a continuous ridge extending from the northeast corner of Haralson County, close to the Polk line, in a southwesterly direction to U. S. Highway 27, about half a mile north of Buchanan in Haralson County. It continues beyond there, changing to a southerly direction, and finally
disappears beneath the Hillabee Chlorite Schist about 3 miles southeast of the center of Tallapoosa in Haralson County. A short way to the west, a unit that seems to be the same quartzite reappears from beneath the Hillabee and makes up Tally Mountain. From the mountain, the quartzite can be traced westward to a cut on Georgia Highway 100, about 2 miles south of Tallapoosa, and then southwestward into Alabama. The quartzite unit crops out along the unpaved roads in the vicinity of Lebanon, Ala., beside the paved road between Abernathy and Plainville, and at several places along the ridges (some of which have fire lookout towers) between Plainville and the prominent ridge north of Abel, in southwest Cleburne County. The quartzite north of Abel is continuous with the Cheaha Sandstone Member of the Talladega Slate on Cheaha Mountain, which extends into the middle of the type Talladega, in Talladega County.

Correlation.-At the beginning of this study, uncertainties arose as to whether the rocks in Polk County that previously had been mapped as Talladega were, in fact, part of that formation whose type locality is about 50 miles away in Alabama. To arrive at an answer, it was decided to determine if units in Polk County or adjacent Haralson County could indeed be traced into the type Talladega.
One unit selected for tracing was a thick section of graywacke that contains distinctive blue quartz pebbles. The graywacke section extends from southeastern Polk County and northeastern Haralson County, westward across U. S. Highway 27, immediately south of the Tallapoosa River. From there it continues southwestward to the town of Tallapoosa, in Haralson County, cropping out on U. S. Highway 78 at the bridge over the Tallapoosa River. Farther southwest, it forms a string of outcrops in Cleburne County, Ala., including the road cut about 5 miles east of Heflin, that can be

The Hillabee Chlorite Schist, which forms the southern boundary of the Talladega in Alabama, also was traced into Georgia. Except for a few short breaks, the Hillabee has a continuous outcrop along the south edge of the Talladega all the way from Talladega County, north-central Alabama, into northwestern Georgia. The Hillabee enters Georgia near the southwest corner of Haralson County and is well displayed where it crosses Georgia Highway 100 in the valley of Walker Creek.
Hydrology.-The hydrologic properties of the Talladega vary greatly within short distances. Wells in phyllite normally yield from less than 1 gpm to about 5 gpm; they average about 150 feet deep. Phyllite containing an appreciable proportion of fracture rock can be expected to yield between 2 and 10 gpm from depths of 50 to 200 feet.
Zones in the Talladega composed primarily of thin-bedded quartzite or graywacke, even though

51

some phyllite is present, yield 10 to 25. gpm, mostly from depths less than 150 feet. Higher yields may be possible where thickly to massively bedded quartzite or graywacke occupy a topographic position favorable to recharge, as along the Tallapoosa River.
Water from the formation is reported to be soft, except for one well, which was said to have moderately hard water. Iron was reported in some wells, but the concentration generally was low to moderate and rarely high.
A few wells drilled close to the escarpment that forms the northern limit of the formation generally have been dry. The topographic break is very pronounced and the escarpment is deeply dissected at short intervals, resulting in a low availability of water.
Because of the prevalent interlayering of permeable and impermeable strata in the Talladega, the principal direction of ground-water movement is along the bedding. For this reason, the strike of the bedding greatly influences well productivity. Wells on strike with a source of recharge, such as a stream, tend to have higher yields because water can pass readily to the well. Conversely, a well drilled across the strike, even though close to a stream, may have a low yield due to the intervening impermeable strata.
GEOLOGIC STRUCTURE
The structure of the geologic formations in Floyd and Polk Counties is chiefly the typical Valley and Ridge type. The rocks are folded into a series of subparallel anticlines and synclines, locally broken by faults. Most of the major topographic features in Floyd County, notably Lavender, Turkey , and Horseleg Mountains, are anticlinal. Rocky Mountain, by contrast, is synclinal having a structure similar to Lookout and Pigeon Mountains in Walker County, Georgia, considered part of the Cumberland Plateau. Indian Mountain in Polk County is a large synclinorium.
Two major thrust faults crossing Floyd County, the Rome Fault and the Coosa Fault, have greatly affected the outcrop patterns of the formations. The Rome Fault, named by Hayes (1891), passes

from the northern part of the county in a zigzag line to Rome, turning westward from there and following an irregular trace into Alabama. The fault is a very low angle thrust that displaced the Conasauga Formation (Cambrian) northwestward several miles over younger formations. The thrusting occurred some time after the deposition of the Floyd Shale (Mississippian).
The Rome Fault can be observed at several places on the west side of the Garden Lakes Subdivision in Rome. Where shale is thrust over shale, the fault zone is very thin, and shows up as a 1- or 2-inch layer of white gouge. Where harder rocks, either siltstone or limestone, are in contact, the fault zone generally is 5 to 10 feet thick and contains a mixture of rocks from above and below. All exposures of the fault zones indicate that it is tight, and offers no avenue for ground-water movement. This was substantiated by data obtained from the well inventory.
Hayes (1891, p. 145) cites abundant evidence that the Rome Fault is a very flat thrust. In view of this, the occurrence of a remnant of the Rome thrust sheet on the northwest side of the major anticline forming Horseleg Mountain indicates that thrusting along the fault preceded the full development of the major folds. The flatness of the thrust plane also means that the Rome Fault did not cause the abrupt termination of the southwardtrending structures forming Horseleg Mountain, the Beach Creek Anticline and Turnip Mountain. These structures were cut off by one or more east-west trending high-angle faults that later were overridden by the Rome thrust sheet. Such east-west faulti.1g was used by Hayes (1891, p. 147) to explain the termination at their south ends of Kincaid Mountain in western Floyd Count~, and Gaylor Ridge and Dirtseller Mountain in adjacent Alabama; they are cut off close to the trace of the Rome Fault.
The other major fault crossing Floyd County is the Coosa Fault, which was given that name by Hayes (1894) because it lies along the south edge of the Coosa Valley. The fault angles northeasterly across the county, bringing the Rome Formation, and in a few places, the Shady Dolomite, up into contact with the Conasauga.
At the only place the plane of the Coosa Fault was observed-beside Spout Springs Road, just southeast of the point where the road crosses Big

52

Cedar Creek-the fault forms a zone several feet thick, made up of a mixture of rocks from above and below. Folding is intense beneath the fault zone, but very slight above it. The fault zone appears to be very tight, and it probably acts as a barrier to the movement of ground water.
Several comparatively short, high-angle faults branch off the Coosa Fault near Cave Spring and bring slices of the Rome Formation upward into contact with the Conasauga and displace the Conasauga up against the Knox Group. Similar faults parallel the Coosa Fault north and south of Rome and cause displacement in the same formations.
The other major fault in the study area, the Cartersville Fault, cuts across the east and south parts of Polk County, moving the metamorphic Talladega Slate into contact with formations of Ordovician age or younger. The fault terminates the southerly structural trends in the formations north of it; rocks on opposite sides of the fault have divergent strikes and, for the most part, are of different lithologies. The trace of the Cartersville Fault is marked by a prominent fault scarp commonly over 100 feet high.
Another east-west fault 7 miles long passes a short way south of Youngs, Polk County, crossing U. S. Highway 27 about 4 miles south of Cedartown. The fault has a displacement of about 500 feet, bringing the Knox Group (Cambrian) up into contact with the Rockmart Slate (Ordovician); it cuts off a large syncline in the Rockmart and Newala near Antioch School and the belt of Newala that extends southward out of Cedartown.
Indian Mountain
The interpretation of the structure and stratigraphy of Indian Mountain has evolved in a rather interesting manner. Earliest workers (Smith, 1890; Hayes, 1892) showed Indian Mountain and the adjacent valley on the southeast to be underlain by Weisner Quartzite of Early Cambrian age. In 1894, Hayes showed the mountain as Weisner Quartzite, but mapped the valley to the southeast as Conasauga. Mter further work in the area, Hayes (1902) revised his map and showed the valley southeast of the mountain as Beaver Limestone (Shady Dolomite of present usage). This interpretation has persisted until the present

(Butt&j 1948), except for Crawford (1957), who mapped the valley as Weisner.
As is discussed in the section on the Frog Mountain Sandstone, lithologic and stratigraphic evidence indicates that Indian Mountain is composed not of Weisner Quartzite, but of Frog Mountain Sandstone and probably younger rocks. The distinctive "birdshot conglomerate" is continuous to the base of Indian Mountain where it overlies the Rockmart Slate and underlies the basal quartzite and conglomerate beds that make up Indian Mountain. As Indian Mountain is a synclinorium, contrary to Hayes' (1902) depiction, the strata on the mountain are stratigraphically above rather than below the rock in the valley to the southeast (now known to be Rockmart Slate and Newala Limestone) and, therefore, are of Devonian age or younger.
Mapping in Cherokee County, Ala., by Cloud (1967) shows that the northwest side of Indian Mountain follows the same stratigraphic sequence as the southeast side: Knox Group, Newala Limestone, and Rockmart Slate. Although past workers, including Cloud, have shown the northwest side of Indian Mountain to be made up of Weisner Quartzite thrust over formations of Ordovician age, further study probably will show that there is no fault and that the sequence is normal from the formations of Ordovician age up through the Frog Mountain Sandstone of Devonian age, and perhaps younger rocks.
The age of the rocks comprising the upper reaches of Indian Mountain has not been det~r mined, and to do so may require considerable field time because of the extreme scarcity of fossils. This much has been learned, however: the beds on the north side of the mountain dip southeasterly, apparently forming the northwest limb of a synclinorium. As can be seen along the road crossing, the mountain from near Bluffton, Ala., to near Hematite Crossing, Ga., the north base of the mountain is formed by light weathering shale, foll<>wed by 100 to 200 feet of sandstone and quartzite that resembles the Frog Mountain Sandstone at Oremont. Above this are 1,000 to 2,000 feet of shale mixed with thin layers of brownweathering siltstone and fine-grained sandstone. At the top of the section is a considerable thickness of light gray, massively bedded quartzite, sandstone, and conglomerate. The lithology and sequence of these units suggest that the lower shale, sandstone,

53

and quartzite is Frog Mountain, the succeeding thick shale section is Floyd Shale, and the upper quartzite is the Hartselle Sandstone Member of the Floyd Shale or other sandstone of Mississippian age, or younger. Sandstone of Mississippian age was mapped by Cloud (1967) a short way west in Alabama.
Etna Valley
The valley southeast of Indian Mountain, extending from the Alabama State line through Etna, Prior, and Oremont to Hematite Crossing, hereafter referred to as Etna Valley, long was one of the principal iron producing centers of Polk County. Iron was mined there as recently as 1955.
Over the years, the structure and stratigraphy of Etna Valley have been given several interpretations. Hayes (1891, 1892) mapped the valley as Weisner Quartzite, but in 1894 showed it as Conasauga, bounded on the north end by Weisner Quartzite. Another chenge came in 1902 when Hayes showed the valley as Beaver Limestone (of former usage), but mapped a narrow strip of Weisner Quartzite along the southeast side. Several workers following Hayes similarly mapped Etna Valley as Shady Dolomite until Crawford (1957) showed it once again as Weisner Quartzite.
During his investigation of the area, Crawford (1957) discovered lithologic and paleontologic evidence that the Newala Limestone and the Floyd Shale were present in the eastern part of Etna Valley. These discoveries, though, were made at the end of his study and Crawford had insufficient time to determine the significance of his finds.
Following Crawford's lead, the writer made additional fossil finds and obtained other data establishing that Etna Valley is entirely underlain by formations ranging in age from Early Ordovician to Mississippian.

UTILIZATION OF GROUND WATER
Ground water, mostly from wells, is used by several thousand rural residents in Floyd and Polk Counties and is the only water available to most of them. Public utilities distribute water in and around the cities and towns and along most of the main roads, but large areas of the counties are totally dependent on ground water. Dairies, chicken houses, egg processing plants, farms, and churches commonly depend on wells.
Industrial demand for ground water has increased manyfold in the past few decades, but where well water is the only source of supply, the demand has largely gone unmet. At Plant Hammond, the Georgia Power Company had to drill three deep wells to get one that would supply 100 gpm. Georgia Kraft Company had several wells drilled in an attempt to develop a supply, but none of the wells was successful. The General Electric Company in Rome investigated the prospects of obtaining 300 gpm from one or more weils: but abandoned the project after deciding that the amount of recharge in the area was insufficient to meet continued withdrawals. Only in the Cedartown area, which is underlain by the Newala Limestone, have wells been able to meet the heavy demands of industry. Wells there are being used to supply 600 to 1,500 gpm.
Spring water, on the other hand, is available in large quantities from springs discharging from the Newala Limestone and the Knox Group, but very little is being used. Aragon Mills is the only industry utilizing spring water and they take several hundred thousand gallons per day from spring 5GGS1 in Polk County.
A somewhat larger volume of spring water is being processed for municipal supplies: Cedartown takes 1.5 mgd from Cedartown Spring, and the town of Cave Spring and the Georgia School for the Deaf are supplied by water from Cave Spring.
WATER-LEVEL FLUCTUATIONS

Th1 The part of Etna Valley around Oremont is a doubly plunging asymmetric syncline cradled in the Knox Group and underlain by the Newala Limestone, some Rockmart Slate, a thin section of Armuchee Chert, the Frog Mountain Sandstone, in one place some Fort Payne Chert, and covered in the center by the Floyd Shale.

Periodic measurements were made on several wells in the study area to ascertain the amount of seasonal fluctuation occurring in the ground-water level. The results show that in flat lying areas that have undergone only minor dissection by streams, the annual fluctuation is in the range of 5 to 10 feet. In more hilly areas where the relief amounts

54

to several tens of feet, the variations range between 10 to 25 feet.
The water levels generally are highest during the months of April and May, and recede slowly to their lowest points in November, December, and January.
Long term variations in ground-water levels resulting from cyclic differences in precipitation over a period of years probably produce changes in the ground-water level, but their extent is not known. The well inventory did not indicate that water levels have dropped significantly; water levels had remained nearly the same for the past 20 to 50 years.
SUMMARY OF GROUND WATER
In all areas of Floyd and Polk Counties, except on steep slopes and narrow ridges, ground water is

available in quantities sufficient to supply a modem home or farm. The chemical quality of the water generally is satisfactory, although in a few localities such impurities as iron may necessitate a filtration system. Wells normally are less than 200 feet deep.
Large capacity wells have been developed in the Newala Limestone in Polk County, and this aquifer offers the best source of industrial well supply. Wells can be developed that will supply 600 to 1,500 gpm.
Springs in Floyd and Polk Counties discharge more than 35 mgd, of which approximately 95 percent is unused except to maintain streamflow. The chemical quality of the spring water is suitable for domestic and many industrial needs. Water samples from six of the largest springs had an average total hardness of 112 ppm and an iron content of 0.05 ppm.

55

REFERENCES

Berry, William B. N., 1960, Graptolite faunas of the Marathon region, West Texas: Texas Univ. Pub. 6005, 179 p.

--- 1964, Geology and ground-water resources of Walker County, Georgia: Georgia Geol. Survey Inf. Circ. 29, 15 p.

Butts, Charles, 1926, Geology of Alabama: The Paleozoic rocks: Alabama Geol. Survey Spec. Rept. 14, p. 41-230.
___ and Gildersleeve, Benjamin, 1948. Geology and mineral resources of the Paleozoic area in northwest Georgia: Georgia Geol. Survey Bull. 54, p.3-79.

Croft, M. G., 1963, Geology and ground-water resources of Bartow County, Georgia: U. S. Geol. Survey Water-Supply Paper 1619-FF, 32 p.
_ _ _, 1964, Geology and ground-water resources of Dade County, Georgia: Georgia Geol. Survey Inf. Circ. 26, 17 p.

Cloud, Preston, Jr., 1967, Geology and bauxite deposits of the Rock Run and Goshen Valley areas, northeast Alabama: U. S. Geol. Survey Bull. 1199-N, p. 1-74.
Conkin, J. E., 1957, Stratigraphy of the New Providence formation (Mississippian) in Jefferson and Bullitt Counties, Kentucky, and fauna of the Coral Ridge member: Bulls. Am. Paleontology, v. 38, no. 168, p. 109-157.
Cooke, C. W., Crickmay, G. W., Butts, Charles, Hays, C. W., Keith, Arthur, McCallie, S. W., 1939, Geologic map of Georgia: Georgia Geol. Survey map.
Cooper, G. Arthur, 1956, Chazyan and related brachiopods: Smithsonian Misc. Colln., v. 127, 1245 p.
Crawford, T. J., 1957, Geology of part of Indian Mountain, Polk County, Georgia and Cherokee County, Alabama: Georgia Min. Newsletter, v. 10, no. 2, p. 39-51.
Cressler, C. W., 1963, Geology and ground-water resources of Catoosa County, Georgia: Georgia Geol. Survey Inf. Circ. 28, 19 p.
___, 1964, Geology and ground-water resources of the Paleozoic rock area, Chattooga County, Georgia: Georgia Geol. Survey Inf. Circ. 27, 14 p.

Culbertson, W. C. 1962, Pennsylvanian nomenclature in northwest Georgia: U.S. Geol. Survey Prof. Paper 450-E, p. 51-57.
Hayes, C. W., 1891, The overthrust faults of the southern Appalachians: Geol. Soc. America Bull., v. 2, p. 141-154.
---, 1892, Geology of northeastern Alabama, and adjacent portions of Georgia and Tennessee: Alabama Geol. Survey Bull. 4, 85 p.
___, 1894, Geology of a portion of the Coosa Valley in Georgia and Alabama: Geol. Soc. America Bull., v. 5, p. 465-480.
_ _ _, 1902, Rome, Georgia: U. S. Geol. Survey Geol. Atlas, Folio 78.
Hurst, V. J., 1953, Chertification in the Fort Payne Formation, Georgia: Georgia Geol. Survey Bull. 60, p. 215-238.
Johnson, Vard H., 1946, Coal deposits on Sand and Lookout Mountains, Dade and Walker Counties, Georgia: U. S. Geol. Survey Prelim. Map.
Keith, Arthur, 1903, U. S. Geol. Survey Geol. Atlas, Cranberry, N. C.-Tenn., Folio 90.
Kellberg, J. M., and Grant, L. F., 1956, Coarse conglomerates of the Middle Ordovician in the

56

REFERENCES-continued

south Appalachian Valley: Geol. Soc. America Bull., v. 67, p. 697-716.
LaForge, L., and others, 1925, Physical Geography of Georgia: Georgia Geol. Survey Bull. 42, 189 p.
Laurence, Robert A., 1961, Report of igneous rock near Rome, Georgia is erroneous: Georgia Mineral Newsletter, v. 14, nos. 2 and 3, p. 3941.
Maynard T. P., 1912, The limestone and cement materials of north Georgia: Georgia Geol. Survey Bull. 27, 293 p.
McCallie, S. W., 1910, A preliminary report on the mineral resources of Georgia: Georgia Geol. Survey Bull. 23, 184 p.
Safford, James M., 1869, Geology of Tennessee: State of Tennessee, Nashville, 550 p.
_ _ and Kil~ebrew, J.B., 1876, The elementary geology of Tennessee: Nashville, 255 p.

Salisbury, John W., 1961, Geology and mineral resources of the northwest quarter of the Cohutta Mountain Quadrangle: Georgia Geol. Survey Bull. 71, 61 p.
Smith, E. A., 1876, Alabama Geol. Survey Rept. Prog. for 1876, p. 11, 23, 25, 42, 207-208.
- - - , 1888, Alabama Geol. Survey Rept. Prog. for 1884-88.
1890, Alabama Geol. Survey Report on Cahaba coal field, p. 133-180.
Spencer, J. W., 1893, The Paleozoic group; Geology of ten counties of northwestern Georgia: Georgia Geol. Survey, 406 p.
Ulrich, E. 0., 1911, Revision of the Paleozoic systems: Geol. Soc. America Bull., v. 22, p. 281680.
Veatch, Otto, 1909, Clay deposits of Georgia: Georgia Geol. Survey Bull. 18, 453 p.
Yochelson, Ellis L. and Bridge, Josiah, 1957, The Lower Qrdovician gastropod Ceratopea: U. S. Geol. Survey Prof. Paper 294-H, p. 281-304.

57

58

APPENDIX A Fossi I Illustrations
59

PLATE 1 Characteristic Cambrian and Ordovician Fossils
Figure 1. Elrathia georgiensis Resser, x l'h. Middle Cambrian, Conasauga Formation. USGS locality 4171CO, outcrop on east bank of Coosa River at the water line at Copras Bluff, 3.5 miles east of Georgia-Alabama state boundary. USNM no. 162542.
Figure 2. Acmarhachis ulrichi (Resser), x 4. Upper Cambrian, Conasauga Formation. USGS locality 4415-CO, a ditch on south side of paved road, about 25 yards west of intersection of road crossing tracks going to Garden Lakes School, south of Club House, Garden Lakes subdivision, Rome, Georgia. USNM no. 162543.
Figure 3. Scaeuogyra cf. S. swezeyi Whitfield, x 1. Upper Cambrian, Knox Group. USGS locality 4417-CO, outcrop on southwest end of Horseleg Mountain (Mount Alto), about 6 miles southwest of the center of Rome, Georgia. USNM no. 162544.
Figure 4. Tricrepicepha/us species, x 2. Upper Cambrian, Conasauga Formation at USGS locality 4415-CO. USNM no. 162545.
Figure 5. Ceratopea tennesseensis Oder, x 2. Lower Ordovician, Newala Limestone. USGS locality 6302-CO, a roadcut along U.S. Highway 278, west of Cedartown; 2.4 miles E of GeorgiaAlabama state boundary and 2.84 miles N of south edge of Rock Run and vicinity quadrangle. USNM no. 162546.
Figure 6a-c. Ceratopea torta Cullison, x l'h. Lower Ordovician, Newala Limestone. USGS locality 6294-CO, waste heap of residuum from an abandoned iron strip mine, at Oremont, 3.3 miles S of the Floyd-Polk County boundary, 0.6 mile WNW of Old Fite School and 0.22 mile E of Southern Railway branch line. USNM no. 162547.
Figure 7. Mcqueenoceras species, x 1'/2. Lower Ordovician, Newala Limestone, at USGS locality 6294-CO. USNM no. 162548.
Figure 8. Allophoceras species, x 2. Lower Ordovician, Newala Limestone at USGS locality 6294-CO. USNM no. 162549.
Figure 9. Ceratopea capuliformis Oder, x 1112. Lower Ordovician, Newala Limestone at USGS locality 6294-CO. USNM no. 162550.
Figure lOa, b. Ceratopea corniformis Oder, x 1. Lower Ordovician, Newala Limestone at USGS locality 6294-CO. USNM no. 162551.
Figure 11. Ceratopea incurvata Yochelson and Bridge, x l 1/2. Lower Ordovician, Newala Limestone at USGS locality 6294-CO. USNM no. 162552.
Figure 12. Ceratopea keithi Ulrich, x 2. Lower Ordovician, Newala Limestone at USGS locality 6294-CO. USNM no. 162553.
Figure 13. Climacograptus cf. C. scharenbergi Lapworth, x 6. Middle Ordovician, Rockmart Slate. USGS locality D1092-CO, 4.9 miles SSW of center of Cedartown, Polk County, Georgia, 0.5 mile south of Pine Bowers Church at intersection of paved and dirt road. USNM no. 162554.
Figure 14. Glossograptus species, x 6. Middle Ordovician, Rockmart Slate. USGS locality D1093-CO, 5.5 miles SW of center of Rockmart; 4.2 miles S of U.S. Highway 278. USNM no. 162555.
Figure 15. Glyptograptus cf. G. teretiusculus (Hisinger) x 6. Middle Ordovician, Rockmart Slate. USGS locality D1093-CO. USNM no. 162556.
Figure 16. Glyptograptus euglyphus (Lapworth) x 6. Middle Ordovician, Rockmart Slate at USGS locality D1092-CO. USNM no. 162557.
Figure 17. Glyptograptus cf. G. euglyphus (Lapworth) x 6. Middle Ordovician, Rockmart Slate at USGS.locality D1092-CO. USNM no. 162558.
Figure 18. Climacograptus aff. C. riddellensis Harris, x 6. Middle Ordovician, Rockmart Slate at USGS locality D1093-CO. USNM no. 162559.
Figures 1, 2, 4, identified by A. R. Palmer; 3, 5, 6, 9-12, identified by E.L. Yochelson; 7, 8, identified by R.H. Flower; 13-18, identified by W.B.N. Berry.
60

6C
17 PLATE 1 Characteristic Cambrian and Ordovician Fossils

PLATE 2 Characteristic Ordovician and Mississippian Fossils
Figure 1. Clymenid trilobite x 3. Middle Ordovician. USGS locality D1408-CO, bedded chert in ditch on west side of paved road, 400 feet S of East Armuchee Church, Catlett quadrangle, Georgia. USNM no. 162560.
Figure 2a-c. Rostricel/ula uariabilis Cooper, x 2. Middle Ordovician, Ridley Limestone. USGS locality 4425-CO, from southwest end of Horseleg Mountain (Mount Alto) on south side and just below crest of saddle that forms main drainage divide; about 30 fl'l't above Upper CambrianMiddle Ordovician contact. USNM no. 162561.
Figures 3, 4. Bathyurus? cf. B.? ex tans (Hall) x 3. Middle Ordovician at USGS locality D1408-CO. USNM no. 162562, 162563.
Figure 5. Helicotoma species, x 1. Middle Ordovician, Mosheim Limestone Member. USGS locality 4128-CO, 2.1 miles NNE of center of Rockmart; 1.1 miles E of Georgia Highway 101. USNM no. 162564.
Figure 6. Loxoplocus (Lophospira) species, x 1. Middle Ordovician, Mosheim Limestone Member at USGS locality 4128-CO. USNM no. 162565.
Figure 7. Nuculoid pelecypod, x 1. Lower Mississippian. USGS locality 21735-PC, from road exposures next to pond, at NE end of dam across Elder's Lake; 6.0 miles SW of center of Cedartown and 1.3 miles SE of old Brewster School. USNM no. 162566.
Figure 8. Goniatites cf. G. hentuckiensis Miller, x 1. Upper Mississippian, Floyd Shale. USGS locality 22703-PC, abandoned iron strip mine about 2100 feet NNE of Oremont r;.ilway crossing, Rock Run quadrangle, Georgia. USNM no. 162566.
Figure 9. Spirifer species. x 1. Lower Mississippian. USGS locality 21731-PC. from chert pit on west side of Georgia Highway 100, 0.7 miles S of its intersection with U.S. Highway 27. USNl\1 no. 162568.
Figure 10. Lepiagonia d. L. analoga (Philips), x 1. Lower Mississippian, at USGS locality 21 731-PC. USNM no. 162569.
Figure 11. Pelecypod allied to Sanguinolites, x 1. Lower Mississippian at USGS locality 21735-PC. USNM no. 162570.
Figure 12. Brachythyrus species, x 1. Lower Mississippian, at USGS locality 21731-PC. USNM no. 162571.
Figure 13. Torynifer cf. T. pseudolineata (Hall), x 11/z. Lower Mississippian. USGS locality 21730-PC. from pit on east side of Georgia Highway 100, 0.4 mile S of its intersection with U.S. Highway 27. USNM no. 162572.
Figure 14. Solitary coral, indeterminate, x 1. Lower Mississippian at USGS locality 21730-PC. USNM no. 162573.
Figure 15. Zaphrentoid horn coral, x 1 112. Lower Mississippian at USGS locality 21730-PC. USNl\1 no. 162574.
Figure 16. Auloporid coral, x 2. Lower Mississippian at USGS locality 21730-PC. USNM no. 162575.
Figures 1, 3, 4, identified by R.J. Ross, Jr.; 2, identified by R.B. Neuman; 5, 6, 11, identified by E.L. Yochelson; 7, identified by J. Pojeta, Jr.; 8, identified by Mackenzie Gordon, Jr.; 9-13, identified by J.T. Dutro, Jr.; 12-14, identified by W.J. Sando.
62

2a 4

3 7

9

10

11

12

;..1.

.\ . ...
...,.. .f 15

PLATE 2 Characteristic Ordovician and Mississippia n Fossil s

64

APPENDIX B Tables
65

Table 1.--Geologic formations and their water-bearing properties, Floyd and Polk Counties, Ga.

System

Rock Unit

Thickness (feet)

Lithology

Pennsy 1vanian Pennsylvanian rocks r undifferentiated
Bangor Limestone

350+ 300+

Thinly to massively bedded sandstone and conglomerate; some shale.
Thickly to massively bedded limestone; some shale at the top.

Mississippian

Floyd Shale; includes Hartselle Sandstone Member at top, limestone unit at base.
Lavender Shale Hember of Fort Payne Chert

1002,000
0-200+

Silt and clay shale, thin bedded siltstone and sandstone. Thickly to thinly bedded sandstone at top; massively bedded limestone at base.
Shale; massively bedded mudstone and impure lime.stone.

Fort Payne Chert

10-200

Thinly to thickly bedded chert.

Devonian

Chattanooga Shale and Maury Member
Armuchee Chert
Frog Mountain Sandstone

8-13 125-+
5-300+

Shale
Thinly to thickly bedded chert.
Thinly to massively bedded sand:5tone and quartzite.

Silurian

Red Mountain Formation

6001,200:t_

Thinly to massively bedded sandstone, shale.

Ordovician

Moccasin, Murfreesboro, Ridley, and Bays Formations undifferentiated
Rockmart Slate

400+ 0-6 OO:c_

Argillaceous limestone, mudstone, sandstone, quartzi te, conglomerate, and shale.
Slate, siltstone, sandstone and conglomerate.

Topography
Limited to Rocky Mountain, Floyd County
Occurs only on flanks of Rocky Mountain, Floyd County, and small area east of there.
Underlies broad valley areas and low hills where sandstone prominent. Hartselle Sandstone forms high ridges.
Flanks of high ridges; broad low ridges, and some valley areas.
Steep ridge slopes; low ridges and rounded hills.
Mainly steep ridge slopes.
Steep ridge slopes, rounded ridges and hills. High ridges and dip slopes
High, generally steep sided strike ridges
Crops out on high ridges, ridge slopes, low hills.
R1dges ana roulng hlUS.

Hydrologic Properties
No data available; probably will yield from 2 to 10 gpm in most low areas, perhaps 50 gpm in center of syncline.
Probably no value as aq11ifer on steep slope; Yields from 3 to 20 gpm in fairly flat areas ,may
supply up to so gpm in low areas near source of
recharge.
Wells in shale and thin sandstone average 80 feet deep, yield from 3 to 20 gpm. Water is soft to moderately hard; nearly half have high iron content. Wells in limestone unit may yield up to 50 gpm.
Wells on gentle slopes and low ridges yield 5 to 50 gpm from depths less than 150 feet. In valleys, yields may be as high as 100 gpm. Water is soft and low in iron content.
Where not steep, wells yield from 8 to 10 gpm. The water is soft to moderately hard; much has a high iron content.
Not an aquifer. Contains iron and sulfide; should be cased off from wells.
Same as Fort Payne Chert.
Wells yield 0 to 10 gpm most areas, depending on topography; up to 50 gpm where thick and recharged by stream.
Wells may supply up to 10 gprn on broad ridge crests; generally not available on narrow crested ridges.
Is an aquifer only in low lying areas of western Floyd County. Wells will yield from 2 to 20 gpm, depending on the amount of sandstone present. Water is soft, but may be high in iron.
Wells average 200 feet deep and yield from 1 to 30 gpm. The water varies from soft to hard, and generally is low in iron content.

Deaton Member of Lenoir Limestone
Lenoir Limestone and Mosheim Member
Newala Limestone

100+ 35+
300+

Ferruginous limestone and sandstone.
Thinly to massively bedded limestone.
Thickly bedded limestone and dolomite.

Valleys Valley areas Forms strike valleys.

Cambrian and Ordovician

Knox Group

Cambrian

Conasauga Formation Eastern belt
Conasauga Formation Western belt
Rome Formation

Shady Dolomite

Cambrian to Pennsylvanian

Talladega Slate

2,0004, 000~

Thickly to massively bedded cherty dolomite; some limestone. Thick chert and clay residuum.

Broad, gently to moderately rolling ridges.

1, 5002:_

Shale and thickly bedded limestone.

Forms strike valleys.

2,000:':.

Shale with limestone units.

Underlies a broad flat valley.

500-
1,000~
30100+
30,000~

Shale and interbedded sandstone, siltstone, and quartzite.
Thick to massive dolomite; some shale.
Phyllite, quartzite, slate, graywacke.

Moderately high strike ridges.
Underlies scarp slopes; one small valley area.
Rolling country; rounded hills, steep valleys.

Not an aquifer~ should be cased off because of high iron content.
Not developed as an aquifer; may supply some water to wells penetrating Rockmart Slate.
Wells average 147 feet; yields generally run 5 to more than 20 gpm; some wells yield up to 1,500 gpm. Water is hard and of good chemical quality. Springs discharge large volumes of water, ranging in volume from 0.5 mgd to 15 mgd. The spring water is moderately hard to hard, low in iron, and is suitable for many industrial uses.
Wells in bedrock average 160 feet deep and yield between 5 and 80 gpm. The water is low in iron and moderately hard to hard. Wells in residuum supply 1 to 15 g:pm; the water is soft and of good quality. Several large springs discharge from this formation.
Wells average 120 feet deep and yield from 2 to 25 gpm, but up to 300 gpm can be obtained from limestone. The water varies from soft to hard, and generally has a low iron content.
Wells less than 200 feet deep generally yield less than 10 gpm; wells 400 feet deep may supply 100 gpm. Dry wells occur. Water varies from soft to hard and some have a high iron and hydrogen sulfide content.
Wells average 100 feet deep; they yield 1 or 2 gpm where mainly in shale, mostly 5 to 10 gpm where sandstone and quartzite are common. Most of the water is soft; some contains high iron.
Not an aquifer on scarp slopes; in valley it probably will supply from 5 to 50 gpm. The water wi 11 be hard, and probably will be low in iron.
Wells generally less than 150 feet deep; yields vary with rock type: 0 to 5 gpm in phyllite; 10 to 25 gpm or more in quartzite and graywa{...ke. The water generally is soft, and the iron content ranges from low to moderate; rarely high.

Well
O< Spn_n(: Number

'.;arne or Owner

Hardness as (Caco 3 ).?_/

Spec1f1c

conduct-

ance

pH

(mlcr:;t

11. s. t' bl1c llea1.tfJ

Floyd '-'ounty

5JJll 5JJ13 SJJ 33 SJJ2l 3JJS4 SKKS1 3JJS1 5JJS2 5HHSl 4HHSl 3GGSl 3GGSl 3GGS2 4HHS2 3JJS2

B1ll ~1cKcllan ',Jllll:3 Hcos., Georg>-a Power Company C. G. Wall Berry Schools Girl Scouts oi Central of Georgia Railroad Morrlson-Camp Groun0 Sor1no Wax Spn ng Harry ,-..:ar1on S?ring Cave S!_,rn:g
do Old Mil::_ Spr1n9 Unknovm .Toe .early

Otk c E'csl Ecsl
or-:k 0k
()k Ok
0% EcJ tcs1

[1

! 2-21-u2

0.7

28

70

2-20-62

42

3-JC-62

13.

411

2-21!-62

lJ.

36

2-20-62

l.l

.8

2-2Q-f,2

.07

l.o

99

3-30-62 J-30 fi2 3-21 f,2 3-2'J".l

14. (,.r

1)3

.11 15

. J5

~ ~

.ll 18

:j .1 2.5

J.C

4.CI J.O

I

7.8

.S

3- 3~- 6 2

7.R

.l'::l J'J

7.7

. 04 25

9.2

.03 ?_7

1.2

12 .

.4

l.l

.6

.o

J ~l

3-20 63

ll.'

J-3( -6?

1.2

3-3Cl-b2

1.5

'.C

.1

'.0

4.0

S.E 15.
!.7

!.0

.2 .2

.4

.5

!.0

2.4

.3 1.2

.0

1.0

.2

3.-: 1.0

.0

131 169 103 ll9
75 97 54 73 82 96 l40 126 128 100 12& 96

153

:2

58

85

53

83 30

52

'i4

77

113

112

109

94

ll'J

220 320 154 190 120 170 66 119 110 141 218 208 210 163 210

7.9 7.7 7.0 7.4 7.0 7.6 7.0 6.9 7.3 7.3 7.7 7.9 7.5 7.4 7.5 7.4

Polk County

(,GG4

14l

3.:>

.6

.c

l87

168

322

SFF9

44

12

75

6.5

3FF34 JFF25
3FF13 JFF15

HolbrooK
w. D. Jar:-~ell
Mead .Jewell Hulsey

Or 40
11'J 481

12. 8.7 .0 .8

4.J

.0

:.L.

4.

.2

.0

3.1

14.

.o

343 109
86 152

276 48

76

144

16

521

8.4

160

5.8

151

7.6

268

7.9

3FF3

W. W. Corn

70

l.6

117

114

212

7.5

SGGJ

Bob Harrison

J30

3. ~

1.3

143

lJC

252

7.6

4GG3

Porter Cr1mes

125

2.2

5.9

110

100

196

7.6

3GG40 5GGS4

R. Campbell Deaton SprinJ

40 l9-f3

2.7
:u.

4.2

29

2.''

2.4

150

1~ 8

36

5.6

217

7.6

4GGS3 Fish Spnng

On

3-20-6"3

6.f 2.)

1 4

3.'1

J.5

100

82

154

7.4

5GGS3 Davette Spring

"3- ~ 'J-r, 3

13.

.6

.8

144

130

215

7.7

SGGSl ]GGSl

Ardgon MJ lls Spr 1ng Cedartown Spr1ng

3-l'J-(3

1.2.

.6

14.

]64

140

I

lO

co

I ::

157

142

232

7.5

264

7.4

3GGS1

do

3-19 63

8.2

14

2 'l

160

136

224

7.7

JFFSl West Spnng

3-20 63

7.1

18

7.1

.9

I

7 : I 7 0 i : 13. 7

74

139

7.2

+-___'-L---~-~ ~~___l__,__ ~I~__~_._o ~ ~ L__--~ 8
L__'F_F_S_3-LY_o_u_ng_s__sp_r_i_ng____________L_____________+-___ i___'-__' o__-0_3__

02 2

4

_ __ L_ _ J J _ . _ i_ _ _ _ _ _L __ _

_L_____

122

18 8 0

__ __- L______L___ _ __ __''_"___ J________L____ _'__

1/ Analyses by c. S. Geological .Survey

!:_I Water 61 to 120 than 181

0 to 60 ppm ~s class1fied "soft" 121 to 180 ppm, "hard" and more

Table 3.--Spring flows in Floyd and Polk Counties, Ga.

Number

Name or Owner

Geologic source

Date
measured or
estimated

Flow (mgd)

Remarks

2GGS1 3GGS3 4HHS2 4HHS3 4HHS4 4HHS5 2JJS2 5JJS1 5,JJS4 5JJS6 5JJS7

Floyd County: Roy Williamon Unknown Unknown Pepperell Mfg. Co. Pepperell Mfg. Co. Pepperell Mfg. Co. W. D. Vann Unknown Hermitage Russell Spring Dempsey Brothers Dairy

5JJS8

Dempsey Brothers Dairy

5JJS10 3GGS2

J. W. Blankenship Mrs. Fred Dodd Mrs. Oline Parker
Old Mill Spring

3GGS4

Cave Spring

4HHSl

Harry Marion Spring

5HHSl Wax Spring

5HHS2

J. R. Abrams

5HHS3 5HHS4

Luther Johnson & neighbors
Dan H. Norton

5JJS2

Morrison Camp Ground Spring

5JJS3

Youngs Mill Spring

5JJS5

Edwards Spring

5JJSll 3JJS1

Harry Dawson Sand Spring

Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation Conasauga Formation

ll/30/62
10/12/50 3/09/64 3/n0/64
ll/09/61 10/26/61 10/26/61 10/12/50 10/25/61

Conasauga Formation 10/25/61

Conasauga Formation 10/25/61

Knox Group Knox Group Knox Group Knox Group Knox Group Knox Group Knox Group Knox Group
Knox Group
Knox Group Knox Group Floyd Shale

5/14/62 ll/16/64
10/ll/50 5/14/62
ll/16/6 4 10/ll/50 10/12/62 ll/16/6 4
10/24/62
10/24/62
10/12/62
10/12/50
ll/18/64 ll/07/50
ll/12/62 10/12/50 ll/12/62 10/26/61 ll/18/&4

0.14 E.

.04 E.

.05 E.

.2

Used by industry

.15 E. Developed

.10 E. Developed

.l4+E. Not used

. 10 E.

.14 E. Supplies 5 homes

.06

Undeveloped

.10 E Used by milk processing plant

.10 E Used by milk processing plant

.07 E

5.

Good industrial

4. 8

supply; would require

large enclosure

2. 4

Supplies water to Cave

2.6

Spring and Georgia

2.5

School for the Deaf

1.3

Undeveloped

l. 2

.9

Seep spring; discharge

from several outlets

.14 E. Supplies water for 5 homes

.14 E. Supplies community

.14 E. Furnishes dairy and 4 homes.

1.6 . 86

Partially enclosed; supplies Morrison Camp in summer

2.

Flows into lake; seep

spring difficult to

protect

2. 3

7

Undeveloped

7

.05 E.

3

Undeveloped

69

Table 3 (cont.) Number

Name or Owner

3JJS2 3JJS5

Joe Early Beard Spring

3JJS7 3JJS9 3JJS10 3KKSl

Berry Schools Mrs. Florence Masingal C. R. Smith Buffington Spring

4KKS2

Arrowhead (Martin) Spring

4KKS3

H. B. Hansard

5LLS3 5LLS4 3JJS3

Ted and Raford Barton Clyde Dunagan Rice Springs Farm

4JJS4

Rice Springs Farm

4JJSl 4JJS2 4KKS1 5LLS1 5LLS2

Berry Schools Berry Schools Crystal Spring Girl Scouts of America Boy Scouts of America

2JJSl 5JJS9 3JJS6
3JJS8

M. S. Clay
William Sims
Central of Georgia Railroad
Thomas Berry Estate

3JJS11 Berry Schools

3FFSl 3FFS3 4FFSl

Polk County: West (deep) Spring
Freeman and William Bentley
E. E. Hudsputh

4FFS2 4FFS4

Unknown J. P. Everett

Geologic source

Date measured
or estimated

Flow (mgd)

Remarks

Floyd Shale Floyd Shale
Floyd Shale Floyd Shale Floyd Shale Floyd Shale
Floyd Shale
Floyd Shale Floyd Shale Floyd Shale Fort Payne Chert

11/16/6 4 10/17/50 10/18/64 10/24/61 10/09/61 10/09/61 10/16/50 11/18/64 10/13/50
9/11/67 10/02/61
10/11/61 10/11/61

Fort Payne Chert

Fort Payne Chert Fort Payne Chert Fort Payne Chert Fort Payne Chert Fort Payne Chert

10/23/61 10/23/61 10/11/61 11/16/64 10/11/61

Ordovician Limestone 11/09/61

Rome Formation

10/24/61

Red Mountain Formation

11/16/64

Red Mountain Formation

11/09/61

Red Mountain Formation

10/23/61

. 3

Undeveloped

1.

Undeveloped

.9

.14 E. Undeveloped

.07 E. Undeveloped

.07 E. Domestic use

.2

Undeveloped

.2 E.

0.30

Supplies Arrowhead Lake

. 47

.10 E. Water used by 2 homes and dairy barn

.04 E.

.03 E.

.60

Flo" measured by

consulting firm

Undeveloped

l.

Flow measured by

Roberts Engineering

Corp. Undeveloped

.07 E. Not used

. 07 E. Stock

. 05 E.

.2 .05 E.

Furnishes water for summer camp
Furnishes water for summer camp

. 07 E.

.07 E.

.1 E.

Flows from pipe and concrete box

.14 E. Undeveloped

.07 E. Undeveloped

Newala Limestone Newala Limestone Newala Limestone
Newala Limestone Newala Limestone
70

8/21/50 11/17/64
4/30/63
10/05/50 11/18/6 4
11/18/64

1.0

Undeveloped. Good

9

location for industry

.007 E. Supplies dairy

3 . 3 E.
3 E.

Undeveloped
Small flow Furnishes home and dairy

Table 3 (cont.)

Number

Name or Owner

4FFS5 "FFSl

E. c. Morgan R. E. Forsyth

3GGS1

Cedartown Spring

4GGS3

Hoyt Beck (Fish Spring)

5GGS1

Aragon Mills

5GGS2

Aragon Mills

5GGS3

Davette Spring

5GGS4

Deaton Spring

3FFS2

R. T. McCoy

4FFS3

Youngs Spring

4FFS6 4GGS1

Philpott Spring Jones Spring

4GGS2

Locke Spring

6GGS1

Paul McKelvey

Geologic source
Newala Limestone New ala Limestone Newala Limestone
Newala Limestone Newala Limestone Newala Limestone Newala Limestone Newala Limestone
Knox Group Knox Group Knox Group Knox Group Knox Group Fort Payne Chert

Date measured
or estimated

Flow (mgd)

Remarks

11/18/64

. 5

Supplies dairy

5/16/63 10/04/50

.28 E. 3. 9

Supplies 3 homes, restaurant and motel
Supplies city of Cedartown

10/18/54

2.9

11/17/64

2.8

I

10/05/50

. 9

3/20/63

. 3 E.

Largely filled in; requires enclosures to protect from
flooding

10/05/50

. 4

Supplies industry

11/18/64

.35

10/05/50

. 7

Undeveloped

11/18/64

. 6

9/26/50

2. 3

11/16/64

2.5

Undeveloped; beside Euharlee Creek but
can be protected from
surface~water

9/25/50 15.6

This measurement made prior to spring being enclosed in concrete and may be the most accurate. Good
location for industry

5/12/66

6.5

Measurement: integrated computation from point velocity readings

6/06/66 10.2

Difference in flow of Euharlee creek upstream and downstream
from the spring

6/06/66

9. 0

Measure of water flowing through pipe
from enclosures; does not include a considerable volume of leakage

4/30/63

. 28 E.

Supplies 2 homes, dairy and chicken houses

10/05/50

. 6

Near railroad;
requires enclosure to protect from surface water

8/21/50

.08 E. Undeveloped

10/05/50

. 4

Undeveloped

11/17/64

. 4 E.

8/22/50

. 3

Undeveloped

11/17/64

. 3 E.

10/06/50

. 2

Undeveloped

71

Table 4.--List of graptolites from the Rockmart Slate, indicated by localities

C2imacograptus ridde22ensis Harris
c. ridde 2 2ensis Harris? c. aff. c. ridde 22ensis Harris c. cf. c. ridde22ensis Harris c. cf. c. scharenbergi Lapworth c. n. sp. (like c. marathonensis) c. sp. (of the c. angu2atus Bulman type) c. sp. (of the c. ridde ZZensis type) c. sp.
Cryptograptus schaferi Lapworth
c. triaor>nis (Carruthers)
Didymograptus cf. D. paraindentus Berry
D. cf. r.. robustus var. norvegiaus Berry
D. cf. D. tornquisti Reudemann G2ossograptus ci Ziatus Enunons?
G. hincksii (Hopkinson) G. sp.
G2yptograptus eug2yphus G. eug2yphus (Lapworth) G. eug 2yphus cf. var. sepos.itus (Keble and Harris) G. aff. G. eug2yphus (Lapworth) G. cf. G. eug2yphus (Lapworth) G. aff. G. eug2yphus var. sepositus (Keble and Harris) G. cf. G. eug2yphus var. sepositus Harris and Keble G. aff. G. teretiuscu2us (Hisinger) G. aff. G. teretiusculus var. siacatus (Ellis and wood) G. cf. G. teretiuscu2us (Hisinger) G. cf. G. teretiuscu2us var. siacatus (Ellis and Wood) G. sp. G. ? sp.
Ha2 2ograptus inutiZ.is (Hall) H. cf. H. mucronatus (Hall)
Isograptl8 sp. (of the I. caduceus type) Pterograptus n. sp. {similar forms occur in the Australian
Darriwil G2yp tog raptus teretiuscu2us Zone) Re tiograp tus aff. R. sp! ei osus Harris R. cf. R. speciosus Harris (one specimen identical
to some from highest Darriwil age locality GZyptograp tus tere tiuscu2us zone in Victoria, Australia) R. sp. R. ? sp. Tri gonograp tus sp.

y
Locality Numbers 1 2 3 4 5 6 7 8 9 10
X

X

X

X

X

X

X

X X

X

X

X

X

X

X

X

X X X X X

X

X

X

X X

X

X

X

X

X

X X X X

X

X

X

X

X

X X
X

X

X

X

X X

X

X X X

X

X

X

X

X

X X

X X
X

X

X

X

X

!I localities described in text.
72



Table 5.--Middle Ordovician graptolite zones of Berry (1960) Locality Number
1 2 3 4 5 6 7 8 9 10

Zone 12 = Climacograp tus bicornis

? ?

??? ?

Zone 11 = Nemagraptus gracilis

? ?

? *? ?

Zone 10 = Glyptograptus teretiusculus * * * * * * * ? * *

Zone 9 = Hallograptus etheridgei

?

? ? ?

* most probable
? possible

73

Table 6.-- Record of wells in Floyd County, Georgia
Geologic symbol: Mb, Bangor Limestone; Mfs, Floyd Shale; Mfp, Fort Payne Chert; Mls, Lavender Shale Member of Fort Payne Chert; MDc, chert of Mississippian and Devonian age; Da, Armuchee Chert; Srm, Red Mountain Formation; On, Newala Limestone; Ok, Knox Group; .Ccd, dolomite of Conasauga Formation; c, shale and limestone of Conasauga (Eastern belt); csl, shale and limestone of Conasauga (Western belt); cls, limestone and some shale of Conasauga (Western belt); cl, limestone of Conasauga; cs, shale and sandstone of Conasauga (Western belt); r, Rome Formation.

Well no.

OWner

2GG5
3GG41 42 43 44 45 46 47 48 49
4GG66 67 68 69 70 7l 72

C. C. Montgomery J. E. Dempsey J. E. Dempsey Glenn Montgomery Mrs. Lois Ellis Shelton Lindsey 0. H. Shaw J. A. Dempsey Mrs. Paul Sewell Mrs. Paul SeweJ.l Roy Tallent Bill Davis W. J. Williams W. J. Williams Miss Ruth Couch
w. B. Justice
Henry H. Jones, Jr. W. L. Duke Clifford Bell R. S. Shiflett
Mrs. A. D. Miller

Type
of well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Dri !led Dri !led Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Slope Hillside Hillside Flat Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope

Drilled

Slope

Geologic
symbol of
aquifer

II Diameter of well (inches)

Depth (feet)

cd-Cr

6 8. 5

csl

214

.Ccls

150

r?

74

r?

70

cd

48

cd

99. 5

cd

72

cd

80

Ccd

65

cd

82

Lower OCk

223

OCk

235

OCk

295

OCk, lower

2 30

Lower OCk

111

OCk

185

OCk, lower

150

c

135

Lower OCk or

161

c-on fault

Lower OCk

96

cased to Water-level (feet) below land
surface

32

24

10

14

10

70

55+

10

33

22

60

36

23

40

20

55

70

175

25

209

111

101

185

150

151

126

95

Date measured
1952
19SG
1961 1962
195 8 195 8 1950
1959 1962 1962
1962
1956

Yield

Use

(gpm)

Domestic and stock

tore ~omestic and stock

Domestic

Stock

15

Domestic and stock

so

Domestic and stock

Domestic

20+ Domestic and stack

None

Domestic and stock

35+ Domestic and stock

Stock

Domestic and stock

Domestic and stock

12

Domestic and stock

Domestic

Domestic

Domestic

Domestic

Domestic

Remarks
Well pumped dry, 3 hours continuous pumping
Water muddies Water muddies Water muddies Water muddies Some iron Some iron Some iron

Table 6 (cont.) Well no.

OWner

4GG 73

74

7S

I

76

SGG63

64

65

66

67

68

69 70

71 2HHl
2 3 4
s
3HHl 2 3 4 5 6

7 8 9 10

c. v. Chisolm
E. Jack Barron E. Jack Barron
s. R. Eden
J. L. Camp J. A. Up the grow J. M. Gribble M. H. Edwards Richard Haney J. A. Ballanger and Clyde Gribble Wallace R. Agon Earl and Charles
Brumbelow
Mrs. D. s. McCluney
Marion Little
w. M. Clemonec c. L. Burnett
H. L. Freeman Joe Allen George Sam Pearson F. E. Western L. L. Puckett T. J. Crews Luther Murphy
M. E. & w. L. Pruitt
and R. L. Jones B. T. Jenkins
w. T. Nicholls s. B. Simms R. c. Vann

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Hillside
Slope Flat Slope Slope Slope Slope Slope Slope

Drilled Drilled

Slope Slope

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Flat Flat Slope Slope Slope Slope Slope Slope Slope Slope Slope

Drilled Drilled Drilled Drilled

Slope Slope Slope Slope

GeoJogic

Diameter Depth Cased to Water-level

Date

Yield

Use

symbol

of well

(feet)

(feet) below land

measured (gprn)

of

(inches)

surface

aquifer

Lower OCk

6

80

80

20

Lower O<:k

6

SOD

128

170

c (?I

6

360

--

--

Lowe::::- OCk

6

140

90

--

Lower ock

6

90

--

so

OCk

6

278

54

30

Upper OCk

6

78

78

38

Upper OCk

6

150

--

52

Upper OCk

6

311

60

--

Upper OCk

6

87

--

--

On

6

139

70

--

Upper OCk

6

179

179

80

Upper OCk

6

160

1SS

--

c

6

126

4S

21

c shale

4

100

--

--

<:c shale

6

llD

20

24

c

6

118

3S

83

c

6

72

20

2S

Mfp

6

162

70

--

Mfp

6

148

100

106

-t:csl

6

125

31

27

csl

6

81

42

21

OCk

6

80

20

14

OCk

6

182

9

20

OCk

6

120

30

--

OCk

6

127

42

46

OCk

6

26S

190

40

OCk

6

80

50

20

1962 1960
-------
1962 1962 1959 1959 ----
----
----
19S6
---1961 ---19S6 1954 l9S9 ---l95S 1960 l9S9 1960 1956
----
1962 1954 1960

--- Domestic

8

Domestic and stock

--- Stock
--- Domestic and stock

--- Domestic

4

Domestic and stock

--- Domestic

16

Domestic

--- Domestic

--- Domestic

14

Domestic and stock

--- Domestic

--- Domestic and stock

--- Domestic

--- Domestic and stock

6

Domestic

4

Domestic and sto.ck

6

Domestic and stock

7

Domestic and stock

--- Domestic

s

Domestic

--- Domestic

--- Domestic

--- Domestic

6

Domestic

lS

Domestic and stock

6

Domestic

lD

Domestic

Remarks Some iron Water muddies

Table 6 (cont.)

Well no.

()I..Jner

3HHll 12 l3 14 15 16
17 18 19 20 21 22 23 24 25 26 27 28 4HHl
2 3 4 5 6
7 8 9
lO

L. F. Bing Clayton White
c. T. Blankenship R. c. Vann c. D. Covey
Alvin Covey
F. M. King
H. c. Cantrell
Jack Montgomery Pine Ridge Dairy
w. D. House
Ed. E. Perkins
Mrs. w. J. Martin J. w. Salmon
Marvin Fortenberry Thurman Chandler Sidney Evans
H. o. Norman
Henry Fincher D. F. Ellis Valley View Rest Home J. J. Rush
w. R. Stephens
Floyd County Board of Education Lawrence Gaus Roy Tillery Pleasant Hope Baptist Church
G. s. Bailey

Type of
well

I

Topography

Geologic symbol
of aquifer

Drilled Dri !led Drilled Drilled Drilled nrilled
Drilled Drilled Drilled Drilled Drilled
Dug Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Slope Slop.e
Slope Slope Hilltop Flat Slope Flat Flat Slope Slope Flat Slope Slope Slope Slope Slope Slope Slope Slope

Drilled Drilled Drilled

Slope Slope Flat

OCk OCk OCk OCk OCk OCk
OCk OCk <:cd tCd cd cd cd csl csl csl csl Mfp-Mfs c Lower OCk c c ;:c Lower Ok
Lower OCk Lower OCk
;:c

Drilled

Flat

c

l

I

Diameter Depth Cased to Water-level

Date

Yi61ld

Use

of well

(feet) (feet) below land

measured (gpm)

(inches)

surface

6

100

20

18

6

300+

24

--

6

102

25

20

6

78

20

15

6

120

21

4

6

75

30

4

6

68

s

s

6

130

15

20

G

100

80

35

6

lOS

30

--

6

53

52

30

48

22

-- I 16

6

57

--

--

6

95

17

85

6

7l

14

--

6

103

--

13.14

6

129

50

--

6

91

60

--

6

67

33

16

6

175

170

154

8

97

--

3S

8

346

40

40

6

186

25

42

6

200

--

--

6

217

200

--

6

372

-

172

6

300

--

--

6

87

87

67

19S8 ---195S 1960 196 3 1959
1955 1962 1957
----
196 2 1962 ---1961 ---19 4S
--------
1950 1962 1959 1961 1955 ----
----
1958 ----
1954

--- Domestic

--- Domestic

10

Domestic

10

Domestic

10

Domestic

1S

Domestic and st_ock.

10

Domestic and stock

60

Domestic

so

Domestic and stock

--- Domestic and stock

10

Domestic

10

Domestic and stock

4

Domestic

60

Domestic

8

Domestic

10+ Stock

9

Domestic

6

Domestic

50

Domestic and stock

--- None

--- Domestic
--- Domestic

--- Domestic and stock

so

Domestic

--- Domestic

s

Domestic and stock

--- Domestic and stock

10+ Domestic and stock

Remarks Milky
Some iron 43 homes This well goes dry at times

Table 6 (cont.) Well no.

OWner

4HHll 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30
31
32
33
34
35 36

F. Pullen H. J. Burkhalter H. J. Burkhalter H. J. Burkhalter F. M. Willis G. T. Haney F. M.Willis Jack Weems Robert Shoemaker
J. c. Price
J. D. Smith D. H. Jones J. D. Kenrick Mrs. Lucille Davis J. R. Roberts St. J. H. Smith J. H. Powell Robert Walther
J. w. Parker
Eddie Crider
R. T. Burchett
Paul Cannon
William Hoffman
Joe B. Mulinix
H. w. Fountain Horace w. Popham

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Flat Slope Flat Hillside Hillside

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Hillside Flat
Hillside Flat
Hilltop Slope Slope Slope
Hillside Slope Slope

Drilled

Flat

Drilled

Slope

Drilled

Slope

Drilled

Slope

Drilled Drilled

Hillside Slope

Geologic

Diameter Depth Cased to Water-level

Date

Yield

Use

symbol

of well

(feet)

(feet) below land

measured (gpm)

of

(inches)

surface

aquifer

Remarks

c - Ok
c c
c ,.
Lower OCk Lower OCk Lower OCk
c c

6

56

28

23

6

187

84

30

6

76

--

--

6

74

--

--

6

110

--

--

6

147

141

117

6

75

--

35

6

148

32

30

6

140

126

80

.:c

6

76

45

--

Cc

6

52

40

8

c

6

120

--

80

c

6

104

67

32

c

6

65

55

--

c1

6

10 8

35

71

c

6

68

50

20

c

6

79

30

31

MDc

6

93

--

76

csl

...6. ,

181

93

35

M1s - on

6

95

33

30

Rome faUlt

cls (flood

6

80

40

20

plain o

river)

MDC - on

6

81

45

24

Rome fault

MDC - on

6

140

40

30

Rome fault

MDc-csl - on 6

130

105

55

Rome fault

cs

6

175

16

16

cd

6

105

--

--

1962 1962 ---------1956 1962 1951 1962
----
1962 1958 1960
----
1928 1962 1956 1958 1959 1962
1962
1957
1960
1948
1963
----

--- Domestic

14+ Domestic
--- Domestic

8

Domestic

15+ Domestic

12

Domestic

15+ Garden

-- - Domestic
--- Domestic and stock

10+ Domestic

8

Domestic

--- Domestic
--- Domestic --- Motel and restaurant

10

Domestic and stock

--- Motel and store

--- Domestic

32

Domestic

5

Domestic

7

Domestic

Water muddies

--- Drinking

--- Domestic

30

Domestic

6

Domestic

8

Domestic

--- Domestic

Drill Uropped 18 feet

Table 6 (cont.) Well no.

Owner

4HH 37 38 39 40 41 42 43 44
5HH1
10 11 12 13 14 15 16 17 18 19 20 21

Jomen w. Terry
T. A. Green A. W. Horton Pepperell Mfg. co. Pepperell Mfg. Co. Pepperell Mfg. Co. Pepperell Mfg. Co. Pepperell Mfg. co. J. T. Traylor K. N. Tate J. A. Ingram J. M. Ingram R. E. Emerson Lewis W. Sullins c. W. Kerce J. E. Abernathy David Vaughn Eugene Evans B. H. Braden Earl Spain Mrs. Lodie Rogers Spring Creek Baptist
Church J. W. Thrash Mrs. G. F. Rogers Tom Carroll John Ellington W. c. Lloyd R. E. Mitchell Grady cook

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled
Dug Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Hillside Hillside
Slope Slope Slope Slope Slope Slope Hillside Hillside Hillside Hillside Slope Slope Slope Slope Slope Slope Slope Hillside Hillside Hillside

Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Hillside Hillside Hillside Hillside Hills ide Hillside Hillside

Geologic Diameter Depth Cased to Water-level

Date

Yield

use

symbol

of well

(feet)

(feet) below land

measured (gpm)

of

(inches)

surface

aquifer

Remarks

Lower OCk Lower Ok
.Ccls

137

120

50

80

78

64

138

43

38

c

2 75

c

153

c

126

c

126

c

75

Lower OCk

120

120

55

Lower Ok

143

143

70

OCk - lower?

41

41

27

Lower OCk

80

70

20

Lower OCk

108

100

75

Lower OCk

104

100

54

Lower OCk

36

60

60

50

Lower OCk?

312

70

60

Lower OCk

4 72

74

100

Lower OCk

120

105

Lower OCk

135

92

Lower OCk

75

75

Lower OCk

130

30

Lower OCk

90

1959 1959 1962
1~60
195 8 1961 1957 19 52 1957 1962 1956 1952
19 59

Domestic

Muddies during heavy

rains

12

Domestic and stock

15

Domestic and stock

Industria)

Industrial

Industrial

Industrial

Industrial

Domestic

40

Domestic and stock

Domestic

10

Domestic and stock

ll

Domestic and stock

20

Domestic

Domestic and stock

20

Domestic and stock

Domestic and stock

Domestic and stock

12

Domestic and stock

Domestic

Domestic and stock

Domestic

Lower OCk Lower OCk Lower OCk Lower OCk Lower OCk Lower OCk Lower OCk

10 3

90

50

126

126

278

70

113

llO

25

92

85

26

87

85

30

10 0

1962
1962 1962 19 52 195 8

30

Domestic

Domestic and stock

17

Domestic and stock

Domestic

60

Domestic and stock

Domestic

20

Domestic

Table 6 (cont.)
Well no.
I

Owner

Type of
"''ell

! Topography
I I

Geoloqic symbol of
aquifer

Diameter of well (inches)

Depth (feet)

Cased to {feet)

Water-level below land
surfaCe

Date measured

5HH 22 23 24 25 26 27 28 29 30
2JJ1 3JJ1
10 ll 12 l3 14 15 16 17 18 19

T. P. Mull B. F. Shell E. R. Brownlow, Jr. G. W. Hall Mrs. A. T. Bailey Leroy Wilbanks Leroy Wilbanks Robert W. Rhyme Mrs. Ruth Litton Q. M. Carroll L. J. Dunaway Lewis B. Payton Howard Cordle Antioch Baptist Church Sara Mcintyre
c. D. Buffington
Howard Mathis
w. M. Cargle G. w. Boggs
G. H. White A. D. Simpson Dewey H. Worthy, Jr. Arthur W. Lloyd
Mrs. Arthur T. Lloyd Rome Kraft
c. W. Apridge c. W. Apridge
C. H. Jonson C. W. Apridge

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Hillside Hillside Hillside Hillside
Slope Slope Slope Slope slope Hills ide Slope slope Slope Slope Slope Slope slope Slope Hills ide Slope slope Flat Flat

Drilled Drilled Drilled Drilled Drilled Drilled

Flat Hillside
Slope Slope Slope Hilltop

Lower OCk Middle Ok Middle OCk
Lower OCk Lower OCk Lower OCk Lower OCk Lower OCk Lower OCk
.Ccsl Mfs or Mls
Mfs Mfs Mfs Mfs Mfs Mfs Mfs. Mfs OCk or Da OCk Mfs Mfs - Cc on fault c Mfs Mfs (?) Mfs (?) Mfs Mfs (?)

120

100

60

136

136

94

446

165

100

293

58

2 30

125

120

167

16 7

122

131

131

24

101

101

60

25.6 7

225

70

84

79

25

84

79

25

85

65

At lsd

60

21

85

12

30

50

42

60

14

69

40

20

65

Flmvs

60

45

17

153

120

60

55

15.33

72

28

15

87

21

205

179

89

157

96

35

359

40
33. 2 8 29.20

1961 1960 1959 1962
1951 1962
1962
1955 1955 1959
1961
1961 1957 1961 1954 1961 1961 1955 1948 1958
1961 1946

Use

Domestic and stack

Domestic

Domestic and stock

Domestic and stock

Domestic

20

None

Domestic and stock

Domestic

Domes tl r:: and stack

Domestic

20

Dcmes tic and stack

20

Domestic and stock

Domestic and stock

Domestic

Domestic

Domestic and stock

Domestic

16

Domes tic and stack

Domestic

Domestic and stock

27

Domestic and stock

10

Domestic

15

Domestic

16

Domestic

6. 5 Domestic

10

Domestic

10

Domestic

None

Domestic

Remarks
Water muddies Water muddies Sulfur
Some iron Some iron Some iron

Table 6 (cont.) Well no.

Owner

3JJ 20 21 22 23 24 25 26 27 28 29 30

31

00

0

32

33

34

35

36

37

38

39

40

4JJl

Jack Apridge George Benton Oliver Montague A. J. Holden Hardin and Holden W. F. Riley ~'i. H. Shakleford W. H. Wood Ray Myers Oconee Clay Products E. T. Coalson
Miss Ruth Bridges Claude H. Haire 0. S. Underwood H. G. Block Georgia Power Co. Rice Spring Farms Rice Spring Farms A. A. Looney C. E. Espy Georgia Power Co. James F. Selman Thomas J. Cordle Jodie Hawkins Harold G. Eleam Max Worley J. Hudson Davis Raymond Davis C. L. Hicks

Type of
well

Topography

Drilled Drilled DrillE'd Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Flat Slope !Jj llside Slope Slope Slope Flat Hillside

Drilled Dri l.Led Drilled Drilled Dri llcd Drilled Drilled Drilled Dr1lled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Sl_ope Flat Flat ll1llside Flat H1lltop Slope Slope slope Flat Slope Slope Slope Slope Slope Slope Slope Slope

Geologic

Diameter Depth Cased to Water-level

Date

Yield

Use

symbol

of well

(feet) (feet) below land

measured (gpm)

of

(inches)

surface

aquifer

Cc Mfs
!'1fs Mfs Mfs Mfs Mfs Hfs Mfs Mfs
Mfs Hfs Mfs l>1ls csl Mfs Mls Srm Mfs Ccsl 'lb Mfs Mfs Mfs Mfs Mfs Mfs Mfs

65

80

21

30

150

21

30

75

18

10

65

20

15

71

29

20

58.5

21

l 5

79

40

30

75

50

12

74

21

30

llO

80

30

96

20

20

121

35

6 8. 5

72.5

66

10

12

411

44. 5

20

152

135

132

159

40

Ground-

level

76

25

8

12

405

15

70

45

25

62

21

170

46

21

21

78

15

7l

21

10

62

21

12

50

42

18

1959 1959 1955 1956 195 7 195 3 1957 19 55 1954 1954 1961 1960
1955
1960
19 55 1961 195 7 1955 1959

10

Domestic

13

None

13

None

Domestic

Domestic

Domestic

18

Domestic

Domestic

Domestic

Domestic

Domestic and stock

10

Domestic

Domestic and stock

Domestic

Domestic

69.6 Industrial

51

Domestic and stock

Domestic and stock

Domestic

Domestic

40

Industrial

Domestic

Domestic

Domestic and stock

Domestic

Domestic and stock

15

Domestic

Domestic

22

Domestic

Remarks
Some iron Some iron Some iron
Flows in winter Flows in winter GGS 259 Some iron Some iron

Table 6 (cont.) Well no.

Owner

4JJ 9 10 11 12 13 14 15 16 17 18 19 20 21
22 23 24 25 26 27 5JJ1
2 3 4 5 6 7 8 9 10

H. E. Thompson Albert Smith Earl Yarborough
c. c. Lynch
Earl Yarborough J. T. Winslett E. 0. Woodfin J. D. Cayle J. L. Hall Roy Selman
c. c. Lynch
Mr. Gresham
c. G. Wall
J. Howard Ford James H. Ellis, Jr. Joe Aycock Idas Adams Pure Oil Company
w. w. Purdy
Jerry Johnson Redmond Ransom A. L. Paris Bill McKellar J. E. Gaines William A. Gaines Jessie Burch J. T. Culberson J. T. Culberson Bill McKellar

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Dri !led Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Slope Slope Slope Flat Slope Flat Flat Slope Slope

Drilled Drilled Drilled Drilled Drilled Dri !led Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Hillside
Flat Flat Flat Slope Slope Slope Slope Slope Slope Slope Slope Slope Flat Flat

Geologic symbol of
aquifer
Hfs Mfs Da 1'1fs Mfs Mfs Ccsl .Ccsl csl csl csl csl r

Diameter lJepth Cased to Water-level

Date

Yield

Use

of we 11

(feet)

(feet) below land

measured (gpm)

(inches)

surface

6

60

6

80

6

86

6

60

6

89

6

66

6

120

6

96

6

80

6

67

6

100

6

94

6

103

30

1

18

6

30

6

21

At 1sd

52

30

--

10

76

10

21

18

40

18

28

14

18

18

18

10

70

18

1961 1957 1961 1961 1954 1961 1957 1959 195 3 19 49 1961 1946 195 7

--- Domestic
--- Domestic and stock

20

Domestic

--- Domestic

10+ Domestic

10

Stock

10

Domestic

--- None

20

Domestic

--- Water grass

--- Domestic

--- Domestic

10

Domestic

c

6

189.51

101

20

r

6

97

92

30

Mfs

6

so

12

15

Mfs

6

10 7

105

82

M1s

6

86

Mfs

6

54

Lower OCk

6

135

26

10

52. 5

--

--

55

c

4

150

150

80

c

6

164

60

30

c1

6

71

24

18

c

6

69

20

15

c

6

85

10

4

c

6

32

32

--

c

6

243

18

15

c

6

50

17

12

c

6

100.6

42

18

1950 1956 195 7 1944 1946
----
1961 1962 1945 1949 19 48 1949 ---19 58 1953 1961

10

Domestic and stock

20

Domestic

10+ Domestic
--- Domestic

12

Domestic

--- Domestic
--- Domestic
--- Domestic

6

Domestic

9

Domestic

15

Domestic and stock

--- Domestic

17

Domestic

--- Domestic

--- Domestic

--- None

Remarks Some iron Some J..ron Some iron
Some iron QW analyses Some iron Some iron Flows in winter

Table 6 (cont.) Well no.

Owner

5JJll 12 l3 14 15 16 17 18 19 20
21 22 23 24 25 26 27 28
29 30 31
32 33 34 35 36 37 38

Bill McKeller Monroe Caine William E. Dawes ,J. R. Dempsey Glenn Davis William Otto Dutton Ben Johnson James T. cJohnson William J. Wesely Floyd County Board of
Education Hubert H. Vaughan ;:\1. V. Crowder J. L. Bishap
c. A. Teague
B. R. Grogan J. T. Stower Henry Sherman Southeastern Pipeline
Company
c. C. Davis & Bro.
C. C. Davis & Bro. Burt Dempsey, Jr.
& Brother Russe 11 Cochran F. A. Webb J. M. Lumpkin Floyd Carner Will Waters J. W. Sherman Willis Bros., Inc.

Type

Topography

Geologic

Diameter Depth Cased to Water-level

Date

Yield

Use

of

symbol

of well

(feet) (feet) below land

measured (gpm)

well

of

(inches)

surface

aquifer

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Flat Slope Slope Slope Slope Slope Flat Slope Hillside Hillside

Drllled Drllled Drilled Drilled Drilled Drilled Drilled Drilled

Hillside Flat
Hillside Slope
Hillside Hillside Hillside
Flat

Drilled Drilled Drilled

Slope Slope Slope

Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Flat Slope Slope Slope Slope Slope Slope

c t.:csl .Ccsl Lower OCk Ccsl .Ccsl or Mfs
r Cr Cr Lower Ok
-c or r -c
Lower OEk Lower Ok Lower Ok Lower OE:'k Lower OE:k -c or Ok
-c -c -c
-c -c Lower Ok Lower Ok -c Lower Ok csl

70

20

10

72

12

81

19.5

12

130

120

60

83

30

23

100. 5

140

80

50

80

14

120

42

30

170

170

110

122

100

40

2 80

12

12

2 09

186

16 7

225

125

478

110

90

150

142

98

160

160

75

36 3

360

10

100

l3

70

12

26

159

16

20

66

40

64

58

148

148

118

136. 5

126

40

130

112

70

135

135

50

30

..1.942 1961 1961 1960 1950
1960 195 4 1961 19 40
1961 1959 1959 1941 1961 1955 1958 1961
1961 19 57 1961
195 7 1960 1960 1950 1957

Domestic

Domestic and stock

10

Domestic and stock

Domestic

Domestic

Domestic

None

Domestic

Domestic

16

School

Yard

10

Stock

5+ Domestic

Domestic

25

Domestic and stock

10

Domestic

15

Domestic

32

None

20

Domestic and stock

Domestic and stock

Domestic

Domestic

10

Domestic

Domestic and stock

9+ Domestic Domestic

10

Domestic and stock

20

Domes tic and stock

Remarks
Water muddies Water muddies Water muddies

Table 6 (cont.)

Well no.

Owner

Type

Topography

Geologic

Diameter Depth Cased to Water-level

Date

Yield

Use

of

symbol

of well

(feet)

(feet) below land

measured (gpm)

well

of

(inches)

surface

aquifer

5JJ 39 40 41 42
3KKl
4KKl
10 11 12 13 l4 15 16 17 18 19 20 21

Willis Bros., Inc. Edna Gaines John Kearse S. :'\!. Whatley Estate of Mabel Duncan Walter Blanton H. T. Davis R. E. Milstead S. I. Storey Lmhr. Co. Benard Storey Storey Lmbr. Co. T. W. Manes T. S. Selman Gordon Scoggins
Carl w. Carney
B. G. Moore
Lee Johnson Thomas W. Hansell H. A. Lindsey Lewis H. Corbin T. E. Stepp Hill Yarborough W. H. Maxey E. E. Perry J. H. Ponder Norman Dew J. H. Hawkins Norman Broom E. All

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Dri !led Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slooe Hillside Slope Slope Hillside Hillside Hillside Slope Hillside Slope Slope Slope Slope 9lope .s.looe

Drilled Drilled Drilled Drilled Drilled Dri !led Dri !led Drilled Drilled Dri !led Drilled Drilled Drilled

Flat Slope Slope Slope Hillside Slope Slope Slope Slope Slope Slope Slope Slope

-csl -cs l Ok -c Mfs or Mls Hfs Mfs Mfs Mfs or Mls Mfs or Mls M1s MOe Mfs Mfs Mfs Mfs
Mfs .\1fs Mfs Mfs Mls (?) Da Da-Mls Mfp Mfs Mfs Mfs Mfs Mfs

42 188 187
60 70 113 64 105 205 130 63 105 83 57 102 55
85 65 60 80 50 48 96 48 102
so
58 87 73

39

10

20

75. 4

l8J

135

30

20

20.30

110

68

44

63

25

205

130

130

30

63

23

42

40

21

20

21

12

30

20

25

15

11

l2

12

Will flow

63

20

18

70

55

21

15

24

20

22.

60

15

1961
1961 1961 1961 1956 19 47 195 7 1954 196 0 1959 19 47
195 4
19 so
1961 19 46 1959 1958 1944 1960

12

Industrial

None

Domestic and stock

15

Domestic and stock

Domestic

Domestic Domestic and stock

Domestic

Domestic

Domestic

Domestic

Domestic

Domestic and stock

20

Domestic and stock

Domestic and stock

52

Domestic

Domestic and stack

20

Domestic

Domestic

Domestic

Domestic

15

Domestic

Domestic and stoc

12

Domestic and stoc

Domestic and stoc

10

Domestic

10

Domestic

Domestic

Domestic

Remarks
Some iron
Water muddy most of time
Some iron Iron, bad taste Some iron Some iron Some iron Some iron Some iron Some iron
Some iron

Table 6 (cont.) Well no.

OWner

4KK 22 23 24 25 26 27 28 29 30 31 32 33 34
5KK1
10 11 12 13 14 15

G. A. Mills A. P. Mills B. A. Duke M. A. Green S. L. Miller Horace Pierce Joe Touchstone James Pasley Mrs. Clarence Willis E. D. Payton Dewey Ellison Frank S. Everett Floyd county Board of
Education Hugh Everett
J. w. Miller
D. W. White Merl V. Williams
D. W. White T. W. Evans Henry Dobinson Eads Estate
Eads Estate R. H. Terry Benny T. Reece C. A. Bird J. c. Young
c. E. Griffin
Horton Estate

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope Flat

Drilled Drilled Drilled Drilled

Slope Slope Slope Slope

Drilled Drilled Drilled Drilled

Slope Slope Hillside Slope

Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Flat Flat Flat Flat

Geologic Diameter Depth Cased to Water-level

Date

Yield

Use

symbol

of well

(feet) (feet) below land measured (gpm)

of

(inches)

surface

aquifer

Remarks

Mfs

Mfs

Mfs

Mfs

Mfs

Mfs

Mfs

Mfs

Mfp

Mfs

Mfp or Mfs

Mfs

Mfs

Mfs

Mfs Mfs Mfs Mfs
Mfs -csl Mfs Mfs or possibly M1 Mfs or Ml Mfs M1s Mfs Mfs Mfs Ccsl

75 93 51. 5 80 165 82. 5 92 45 47.5 50 52.5 50.5 344
72 85 82 123
80 75 108 113
110 65 55 85. 5 53 60 85

34 30 20 60
19
25
21 100
21 18 21
63 42 16 42 30 42 21
20.5 38 85

50 17 25
21
18 15 12 10 150 12 35 16 40
11.44
14.19
15

1961 1961 19 56
195 3
1959 1955 1957 1952
1961 1954 1961 1960
1961
1961
1961

18

Domestic

20

Domestic and stack

Some iron

16

Domestic

Some iron

Domestic Stock

Some iron

10

Domestic and stock

Domestic

10

Domestic

Domestic and stock

Domestic

Domestic

Domestic

21

None

Not sufficient yield for year-round use
Some iron High iron, lime

Domestic Domestic and stock Domestic Domestic and stock
Domestic and stock Domestic Domestic None

Some iron Some iron Some iron Some iron
Some iron Some iron

Domestic

Domestic

Domestic

Domestic

Domestic

20

Domestic and stock

Domestic and stock

Some iron Some iron
Some iron Some iron

Table 6 (cont.) Well no.

Owner

5KK 16 17 18 19 20 21
2JJ1 4LL1 5LL1

Henry Ratliff
s. J. Whatley
M. K. Babb Homer N. Smith
c. L. Autry
Mrs. Annie Lee Nix Q. M. Carroll Hugh Treadaway Rome Hatchery Rome Hatchery Weldon Touchstone

00 at

Type

Topography

Geologic

Diameter Depth Cased to Water-level

Date

Yield

Use

of

symbol

of well

(feet)

(feet) below land

measured (gpm)

well

of

(inches}

surface

aquifer

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope slope Flat Slope Slope Slope Hillside Hillside Slope Slope Slope

.c or tel cs c c c -c -ecsl Mfs

95

30

18

Domestic

60

20

5.80

1961

Domestic

85

12

1956

11

Watering grass

52

52

15

1961

Domestic and stock

77

77

20

1961

Domestic and stock

92

92

Domestic and stock

225

70

Domestic

60

60

48

1954

Domestic and stock

146

14

1960

Domestic and stock

46

21

10. 45

1961

Domestic and stock

92

20

20

1961

Domestic and stock

Remarks Flows during winter

Table 7.-- Record of wells in Polk County, Georgia.
Geologic symbol: Mfs, Floyd Shale; Mfp, Fort Payne Chert; Ors, sandstone and conglomerate in Rockmart Slate; Or, Rockmart Slate; On, New ala Limestone; OCk, Knox Group; Cc, Conasauga Formation; Tu, Talladega Slate, undifferentiated.

Well No.

Owner

2FF1
3FF1
10 11 12 13 14 15 16 17 18 19 20 21 22 23

Herman Hill Jud Bozier Max Harden Ed Williams Emmett Laurens Paul Watson Andy Donaldson
I. w. Pruitt R. c. Pruitt w. w. Corn
W. W. Corn Louis Hajosy C. & S. Breeding Farm W. J. Knight H. E. Wood
w. s. Watson
Paul Rainey H. D. Pope Lumus Dingler E. M. Head J. I. Casey Jewell Hulsey Thomas Wray
T. D. Wray
David Powell Arthur Garmon Edward Dyer Homer Hackney J. c. Covey R. D. Byron

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Slope Hill top Hillside Slope Slooe Slope Slope Hillside Hillside Hillside Slope Slope Hill top Hillside Hillside Slope Slope Hillside Hillside Slope
Flat Slope Slope
Flat SloPe Slope

GeOlogic symbol of
aquifer OCk OCk On On On On On
On-OCk
OCk On On On On On On OCk Or On on OCk Or On Or Or
or
Or Or Or

Diameter Depth Cased to Water-level

Date

Yield

Use

of well

(feet)

(feet) below land

measured (gpm)

(inches)

surface

135.0

135. 0

206. 5

149

111

95

95

30

93

58

2 76

60

dry

200

185

30

93

93

40

155

101

50

70

70

35

69

69

20

180

160

60

85

85

55

52

52

20

107

89

30

75

60

37

88

65

81

81

30

100

40

18

119

55

265

32

487

85

45

78

12

13

52

30

20

55

55

11

90

20

25

92

21

15

55

21

16

56

10

60

50

15

1948

Domestic and stock

Domestic

Domestic and stock

Domestic

None

10

Domestic

70

Domestic

Domestic

15

Domestic

10

Domestic and stock

Domes tic and stack

Domestic

15

Domestic and stock

Domestic

Domestic

10

Domestic and stock

10

Domestic and stock

Domestic

10

Domestic and stock

Domestic

Domestic and stock

15

Domestic and stock

18

Stock

10

Domestic and stock

18

Domestic and stock

10

Domestic and stock

Domestic and stock

18

Domestic and stock

10

Domestic

Domestic and stock

Remarks
QW analysis
QW analysis Sulfur Some iron Some iron

Table 7 (cont.)

I

Well no.

Owner

Type

Topography

Dlameter Depth Cased to Water-level

Date Yield

Use

Remarks

of

of well

(feet)

(feet) below land

measured (gprn)

weLl

of

(inches)

surface

aquifc'r

~-----+--------------~-------+--------~-------+----~r----+-----4--------~-----4----+-------------~---------------

3FF 2 4

W. F. Knight

Drilled

Slope

Or

55

15

30

Domestic

Some iron

25

W. D. ,Jarrell

Drilled

Slone

40

16

15

25

Domestic

Some iron - QW analysis

26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 4FF 1
10 ll

0. L. Culp G. B. Lee, Jr. C. L. Wright Preacher Howard Lavey Davis Arthur Blythcr
l'l. c. Holbrook
John M. Forrister W. M. Holbrook Wiley Casey Tona Sawyer Homer J. Carnes Lester Commor H. A. Von Husyer John Brach
Louis s. Hajosy
William Whitfield J. J. Lassiter Amos Hudson, Jr. Scott Dollar Wallace Simpson Jarnes Keil Joel Atkins M. W. Lee E. M. Ste.vart
,Jack Sharp \Varren Gifford

Drilled Dd lled Drilled Drilled Drilled Drilled Drilled Dd lled Drilled Drilled Dri 1led Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Dri] led Drilled Drilled Drilled Drilled Urilled

Slope Slooe slope Slooe Slope
Flat Slope Slope
Flat Slope s1ore Slope
Flat Slope Slope
Flnt Slope Slope Slope Hillside Flat-valley Slope Slope Slope SloPe Slope Slope

Or On Or Or Or Or On On Or On On Or OCk Or On On Or OCk On Tu On Or OCk Or 0n+Or at top
On

103 391 161
63 70 26.5 90 113 39 97 430 114 130 54 100 70 190 200 410 12 8 115 78 90 196 212 140 78

36 30
10
87 40 104
34 40 40 20 l3 52 28
78 40 100+
30

22 81
4. 66 15 18 18.7 25 20
3. 62 24
45 30 37 50
40 61

194 8 194 8 1948 19 48
1948

Domestic and stock Some iron

Domestic and stock

Domes tic

Domestic

Domestic

Domestic

Domestic

Domestic

Domestic

Some iron

75

Domestic and stock

ll

Domestic and stock Some iron

Domestic and stock Some iron

Domestic

15

Domestic

Domestic

Domestic and stock

11

Domestic

80

Cannery

Domestic

10

Domestic and stock Some iron

Domestic

15

Domestic

Domestic

30

Domestic and stock

10

Domestic and stock

10

Domestic and stock

Domestic

Table 7 (cont.) Well no.

Owner

4FF 12

13

14

15

16

17

18

19

20

21

22

23

00

24

00

25

26

27

28 SFF1

10 ll 12

Robert Grogan Polk County Nat Campbell Wesley Atkins Billy Campbell Mrs. Marco Davis R. L. Grogan Tom Mullen L. 0. Lawrence Gammage Canst. Co. Doyle Baldwin Seaboard RR Walt Chandler Charles Wood
c. A. McBurnett
Cedartown Rod and Gun Club
Don Norris Oliver Wood
Lowell c. Hiatt
Hoke Thompson F. 0. Barrow Mrs. John I. Davis H. L. Brumbelow Bill Miller
F. w. Waters
Walt Chandler J. W. Stegall W. c. Jacobs J. R. Hutchison

Type

Topography

Geologic Diameter Depth Cased to Water-level

Date Yield

Use

of

symbol

of well

(feet) (feet) below land

measured (gpm)

well

of

(inches)

surface

aquifer

Drilled 1

Nat

On

Drilled

Flat

On

Drilled

Slope

On

Drilled

Slope

Or

Drilled

Slope

on

Drilled Foot of hil

Ok

Drilled

Slope

On

Drilled

Slope

Ok

Drilled

Slope

OCk

Drilled

Slope

On

Drilled

Slope

On

Drilled

Slope

On

Drilled

Hillside

Or

Drilled

Flat

On

Dug

Foot of hi!

Tu

Drilled

Hillside

Tu

250

50

225

40

65

40

165

20

15

240

59

58

91. 8

38

19 8

19 8

60

52

42

20

74

74

39

160

5. 19

9 8. 5

33

15

23. 2

ll. 82

126

126

150

150

28

120

125

18

19 48 1952
1948 1948 1962 1962

l/2 Domestic

11

School

Domestic

Domestic

Domestic and stock

Domestic and stock

Domestic

Domestic and stock

20

Domestic and stock

Domestic

30

Domestic

Domestic

10

Domestic and stock

Domestic and stock

Stock

3 l/2 Domestic

Drilled Dug Dug Dug
Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Hillside Hillside Hillside
Slope Slope Slope Slope Slope Hillside Hillside Slope Slope

Ok-On Tu Tu Tu OCk
on
OCk OCk On Ors Ors Or Or

100

62

29

30

48

51

40

36

23

18

135

115

80

312

292

83

80

107

107

95

67

57

20

150

14

30

44

15

23.13

80

25

so

106

17

1948

60

Domes tic

Domestic

Domestic

Domestic

Domestic and stock

Domestic and stock

10

Domestic and stock

Domestic and stock

10

Domestic and stock

10

Domestic and stock

Domestic and stock

Domestic

Domestic and stock

Remarks
Some iron Some iron
Some iron Some iron Some iron Some iron

Table 7 (cont.) Well no.

Owner

5FF 13 14 15 16 17 18 19
6FF1 2GG1
3GG1
10 ll 12 13 14 15 16

Wm. Paul Dumas and Wayne Yates
Ralph o. Jackson, Jr.
Ralph 0. Jackson, Jr.
Fred White Robert Forsyth Robert Forsyth Walter L. Baines Dorsey Jones J. P. Shaw J. P. Shaw Jane Hicks and
Stovall Trawick C. N. Dougherty J. D. Beck T. A. Willingham Luther Dempsey George Rice Robert Campbell Polk County Ben Parrish J. A. Kilpatrick M. W. Youngblood Mrs. Lola Wingate Glen carter Mrs. c. V. Shost John Redding Mrs. Christine Smith J. B. Green N. W. Sorrells

Type

Tnpography

Geologic

Diameter Depth Cased to Water-level

Date Yield

Use

of

symbol

of well

(feet) (feet) below land

measured (gpm)

well

of

(inches)

surface

aquifer

Drilled

Slope

Ors

126

100

15

1 1/2 Domestic

Drilled

Hillside

or

100

100

70

Drilled

Slope

dolomite? and cheit?

186

80

80

Dug

Slope

Tu

48

57

57.5

Drilled

Hillside

On

376

60

60

Drilled

Hillside

Or(?)

196

196

50

Drilled

Hillsic1e

Ors

107

65

67

Drilled

Hi 11top

Tu

130

95

90

Drilled

slope

Ok residuurr

60

60

30

Drilled

Slope

OCk

162

162

50

Drilled Flat-valley

Mfs

130

130

75

1964

Domestic 'oomestic and stock

Domestic

10

Domestic and stock

10

Domestic and stock

10

Domestic

Domestic

Domestic and stock

30

Domestic and stock

Domestic and stock

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Flat-valley Flat Flat Flat Slope slope Slope Slope Slope Slope Slope Slope Slope slope Slope Flat Slope

Mfs c OCk OCk OCk
OCk-On OCk OCk OCk
OCk OCk OCk OCk OCk On OCk

130 55
101 49
274 200 205 183
57 72 57 80 218 137 182 53 145

130 55
100 49 65
183 52
57 70 84 60 182 15 145

30 14 61 27
49.08 100 150
15
20
76 150

1948

10

Domestic

28

Domestic and stock

Domestic and stock

Domestic and stock

Domestic

None

12

School

12

Domestic

None

Domestic and stock

10

Domestic and stack

20

Domestic

Domestic

60

Domestic

Domestic and stock

10

Domestic

Domestic

Remarks
Some iron Some iron
Some iron Some iron Some iron Some iron

Table 7 (cont.) Well no.

Owner

3GG 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38
39
40 4GG1

Clarence Drumond Joe M. Collier Avery Gossett
s. C. Madden
H. E. Odom Ted Smith W. H. Dempsey T. W. Thompson Fred Sprayberry W. R. Robinson W. R. Robinson Robert H. Witcher James Strickland M. Mannus James F. Green Mrs. G. C. Green H. W. Bedford Paul Heard B. W. Edwards M. Teal T. F. Atkins C. W. Zuker
Napea Chemical Co.
Robert Campbell Georgia Forestry Conun. H. M. Isbell Porter Grimes Guy Rutland Betty Stucher

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Hilltop Slope Slope Slope Slope Slope Slope Slope Slope Slope Hillside Slope Slope .Slope Slope Slope Flat Sloi_Je Slope

Drilled

Flat

Dug Drilled Drilled Drilled Drilled Dr.i lled

Slope Slope Slope F'lat Hillside Flat

Geologic symbol of
aguifer

Diameter of well (inches)

Depth (feet)

Cased to (feet)

Water-level below land
surface

Ok OCk OCk OCk
OE:k OE:k OE:k On On OCk OCk OCk OE:k OCk OCk OCk OCk OE:k On On Ok OCk On
OCk
Ok OCk OCk

82

82

85

125

93

93

66

30

110

98

132

84

57

32

80

25

100

100

100

100

35

100

100

50

217

175

100

134

169

169

109

158

158

136

87

60

26

215

207

440

70

40

32

20

62

22 .12

100

60

10

7 3

42

20

48

40

100.5

90

167

17

12 8

12 8

90

99

45

89

89

Date Yield

Use

measured (gpm)

1948

Domestic and stack

Domestic

Domestic

18

Domestic and stock

Domestic

25

Domestic

Domestic and stack

15

Domestic

Domestic

10

Domestic and stack

10

Stock

10

Domestic and stock

10

Domestic and stock

Domestic

Domestic and stock

Domestic and stock

10

Domestic

10

Domestic

12

Domestic and stock

10

Domestlc

Domestic

Domestic

1500 'Industrial

Domes tic

Domestic

Domestic and stock

10

Bath

Domestic

Remarks Some iron
Some iron Some iron
Some iron Some iron

Table 7 (cont.) Well no.

Owner

4GG 6
10 ll 12 l3 14 15 16 17 18 19 20 21 22 23 24 25 26 27 213
29 30 31 32 33 34

Jirrunie 0. Camp Glenn Ledford J. W. Wills Henry Godwin, Sr. R. R. Morgan Polk County M. C. Stringer Harper Home Farm Unknown Polk County Eugene Drumond J. W. Wood Oscar Welchel! Mrs. Chapple Juice Stanley Arnold Hugh Deems J. E. Isham
w. F. Davis
R. F. Casey Mrs. Noble Holland H. B. Simpson V. 0. Stewart H. W. Trawick
S. w. Trawick
W. G. Hice B. F. Drurrunond Mrs. E. T. Faires FHA T. v. Pilgrim, Sr.

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Hillside Hillside
Slope Slope Flat Flat Slope Slope Hillside Slope Slope Hillside Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope Hillside

Drilled Drilled Drilled Drilled Drilled Drilled

Hillside Slope Slope
Hillside Hillside
Slope

Geologic symbol of
aqui fer

Diameter of well (inches)

Depth (feet)

Cased to Water-level (feet) below land surfa-ce

Ok Ok -c Ok -c -c -c -c -c Ok Ok Ok OCk OCk Ok -c Ok Ok Ok -c
-c
Ok

206.5 200
68 67.3 111 208 47.5 104 112 185 71 98.5 52 42 107 216 120 127 86 96 103 101 360

206.5 200
61 67 41 120 4 7. 5 90 112
61 88.5 52

150 20 55. 93 25 70 12. 5 90.46 70 60 31 6 8. 5 40 32. 8

2l

66

120

12 7

77

76

40

87

33

50

180

Ok

85

Ok

158

155

60

Ok

2 80

2 80

100

Ok

195

195

40

Ok

251

151

70

OCk

90

75

Date Yield measured (gpm)
20 19 48
l3
19 48
10 16
1945
10 10 10 14 10 15
20

Use
Domestic Domestic Domestic Domestic Domestic School Domestic Domestic and stock Domestic School Domestic Domestic Domestic and stock Domestic Domestic Domestic and stock Domestic and stock Domestic and stock Domestic Domestic and stock Domestic and stock Domestic and stock Domestic
Domestic and stock Domestic and stock Domestic Domestic None Domestic

Remarks
Some iron Salty taste Some iron

Table 7 (cont.) Well no.

Owner

4GG 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59
60 61 62 63

Herbert Dollar John A. Austin
Rupert w. Herndon
Billy Austin M. M. Casey R. E. Blair J. W. Long Mrs. Dora Edwards W. B. Early
w. H. Blanchard
J. E. Wesson Harry Lumpkin J. B. Willingham Luther Boling Keith L. Lawllass J. S. Holland Oil Barnett Sammy King Calvin Bell A. C. Garrett, Jr. Rayford Deemes Jim Cook James F. Crawford Mrs. W. L. Wilkerson Billy Wilkerson
Charles Blair R. F. Spanger
w. M. Zuker
M. Lindsey

Type of
well

Topography

Drilled Drilled Drilled Drilled Drilled Drilled Drilled, Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Slope Slope Slope Hillside Slope Hillside Hillside Hillside Flat Flat Slope Slope Slope Slope Slope Slope Slope Hillside Hillside Hillside Hillside

Drilled Drilled Drilled Drilled

Hillside Slope Slope Flat

Geologic symbol of
aquifer

Diameter of well {inches)

Depth (feet)

Cased to {feet)

Water-level below land
surfa-ce

OCk OCk OCk OCk
Ok OCk OCk OCk OCk
OCk OCk OCk -f'c -f'c OCk OCk
OCk
on
0-f'k Ok

128 128 126 270
81 104 135 165 153 22 4. 5 160 167 120
50 115
99 147 110 140 122. 5 160 155
80 267
90

128

60

] 30

110

126

56

190

172

81

25

104

59

60

100

133

138

100

16 7

114

88

42

22

115

40

70

54

35

87

110

18

140

90

117.5

40

4 7

110

155

80

40

165

16 7

78

45

OCk OCk -f'c -c

91

91

90

DO

67.4

83

83

41

83

54.77

Date Yield

Use

measured (gpm)

1948 19 48

Domestic and stock

Domestic and stock

Domestic and stock

10

Domestic

25

Domestic and stock

10

Domestic and stock

Domestic and stock

Domestic

10

Domestic

!James tic

Domestic

Domestic and stock

12

Domestic

10

Domestic

10

Domestic and stock

15

Domestic

20

Domestic

Domestic and stock

12

Domestic and stock

Domestic and stock

30

Domestic and stock

20

Domestic and stock

Domestic and stock

Domestic and stock

10

Domestic and stock

10

Domestic .and stocK

35

Domestic and stock

Domestic and stock

Domestic and stock

Remarks Some iron

Table 7 (cont.) Well no.

Owner

4GG 64 65
5GG1 2 3 4 5 6
7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23
24 25 26

Roy Adams Uxbridge Division of
Indian Head Mills Bob Harrison
E. c. Johnson
Jack Campbell Elmo Pepper R. K. Brernbelow
c. B. Nettler
Belle View Church Paul McCown Gi !bert Campbell 0. L. Smith Alvis Miller, Jr. B. E. Golden G. A. Fuchs E. M. Herring Mrs. May Bennett A. F. Jackson Mrs. Horace Williams Charley Fanin Dock Moates J. A. Abernathy R. H. Bond Paul Morgan I. Gentry
Roy Hu9hes
s. J. Noland
Cleo Brown

Type of
well

Topography

Drilled Drilled

Hillside Slope

Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Slope Slope Slope Hillside

Dug Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled Drilled

Slope Slope Hillside Slope Slope Slope Slope Slope Slope Slope Slope Slope Slope Hilltop Slope Slope Slope

Drilled

Slope

Drilled Drilled

Slope Hillside

Geologic symbol of
aquifer

Diameter of well (inches)

Depth (feet)

Cased to (feet)

Water-level below land
surface

Ok

6

83

22

15

On

10

190

80

60

Ok

6

Ok

6

Ok

6

Ok

6

Ok

6

On or top

6

of Ok

Ok residuun 48

Ok

6

Ok

6

On

6

Ok

6

On

6

On

6

on

6

On

6

On

6

On

6

On

6

On

6

On

6

OCk

6

On

6

Ori

6

On

6

On

6

Or

6

130 118.5 121 114 146.5 105
17 130 229.5
77 137
82 54 151. 5 129 359 10 3 150 60 186 290 109. 5 76 83
219 143

130 118. 5 121 112 146 105
--
100 68 72 75 70 7 14 30 34 35 75 46 38 40 54 60 60
16 139

60 36 81 75 46 65
19. 0 65 99 -54 42 13 48
--
20 43 86 30 45 40.96 58 55 25
18 100

Date Yield

Use

measured (gpm)

----
----
----
----
----
----
----
----
1948
----
-------
----
-------------------
----
-------
1946
----
----
----
-------

30

Domestic and stock

650

Industrial

8

Domestic

9

Domestic

5

Domestic

--

Domestic

--

Domestic

--

Domestic

--

Church

--

Domestic

--

Domestic and stock

10

Domestic and stock

10

Domestic

8

Domestic and stock

--

Domestic and stock

--

Domestic and stock

-- None

20

Domestic and stock

10

Domestic and stock

4

Domestic

10

Domestic and stock

5

Domes tic

-- Stock

6

Domestic and stock

4

Domestic

10

Domestic

--

Domestic

10

Domestic and stock

Remarks
Some iron QW analysis

Table 7 (cont.)

Well no.

Owner

Topography

Geologic Diameter Depth Cased to Water-level

Date Yield

Use

symbol

of well

{feet) {feet) below land

measured (gpm)

of

{inches)

surface

aquifer

Remarks

SGG 27

L. W, Spinks

Drilfed

Slope

Or

172

172

75

Domestic

28

H. I. Brock

Drilled

Slope

On

105

40

45

Domestic

29

L. C. Carlton

Drilled

slope

On

444

44

44

16

Domestic and stock

30

J. R. Terry

Drilled

Slope

On

308

208

100

20

Domestic and stock

31

J. H. Fincher

Drilled

Slope

On

90

34

54

10

Domestic

32

James Harvey

Drilled

Slope

On

165

162

75

Domestic and stock

33

Roy Forsyth

Drilled

Slope

On

94

94

Domestic

34

Bill Dover

Drilled

Slope

On

25

20.6

1948

Domestic

35

Rube Engle

Drilled

Slope

On

249

100

99

Domestic

36

Albert W. Ingle

Drilled Hillside

On

106

17

l3

Domestic and stock

37

Southern Railway

Drilled

Slope

Ok

89

Domestic

38

J. W. Pinkard

Dri !led Hillside

Ok

83

81

33

20

Domestic and stock

39

John Davis

Drilled Hillside

Ok

101

21

40

Domestic and stock

40

Jimmy Strange

Drilled Hillside

On

12 3

123

43

30

Domestic

41

T. K. Davi tte

Drilled

Slope

On

64

40

20

10

Domestic and stock

42

D. H. Lewis

Drilled

Slope

On

48

30

20

10

Domestic

43

W. C. Deaton

Drilled Hillside

On

117

67

so

10

Domestic and stock

44

Will M. White

Drilled

Slope

On

120

44

44

20+ Domestic and stock

45

R. B. Arp, Sr.

Drilled

Slope

On

72

64

30

15

Domestic and stock

46

George Baine

Drilled

Slope

On

106

40

44

Domestic

47

James L. Lowell

Drilled

Slope

Ok

450

38

44

Domestic and stock

48

John H. Morgan

Drilled

Slope

Ok

67

67

12

Domestic

49

Mrs. w. M. Jones

Drilled

Flat

On

85

77

10+ Domestic and stock

so

Harry Wright

Drilled

Slope

Ok

120

100+

10

Domestic

51

Calvin Fredick

Drilled

Slope

Ok

241

80

61

Domestic and stock

52

Tom Fitzpatrick

Drilled

Slope

Ok

134

134

Domestic and stock

53

Raymond Mull

Drilled

Slope

OCk

90

90 I 70

.Jomestic and stock

L----5-4----~-T_. kk----~---------L--2_7_5 L-~~5------4---------~------~-D-o_m_e_s_t_i_c ~ 55

H.

_

_EB_.._WC_h_lal_.rt_ke_s_i_d_e__

_

_

_

_

_

_ i

_ _

_DD_rr_ii_lll_el_ed_d_L_

_

_SS_ll_oo_pp_ee_

_

_

_ L

_ _

_

_

'~
_:_:_

L i 34___L___l_l_5__

-

None

_ _ _ _ _ _ _ _ _ _L -_ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _

Table 7 (cont.) Well no.

Owner

SGG 56 57 58 59 60 61 62
6GG1
~
c:.n

Charles Dansby
Fred Pinkard Tyrus Jones P. R. Garnett Cecil Kite Clyde Tillery Howard E. Davis D. E. Waldrop
Mrs. J. w. Waldrop
Estate Ivey Waits
c. s. Smith c. T. Cagle
Ivey Evans

Type of
well

Topography

Geologic symbol of
aquifer

Dlameter of well (inches)

Depth (feet)

Cased to (feet)

Water-level below land
surface

Drilled Dri !led Drilled Drilled Drilled
Dug Drilled Drilled Drilled

Slope Slope Slope Slope Slope Flat Flat Hillside Slope

Ok

Of:k Ok

OCk

()k

Of:k

36

OCk residuum

On OCk

142 240 136 142 186
22 135 152. 5 106

115

210

136

90

142

26

186

126

10

152.5

94

106

56

Drilled

Hill top

Mfp

Drilled

Slope

Mfp

Drilled

Slope

On

Drilled

Slope

On

76

76

125

80

lOS

186

120

250

177

Date Yield measured (gprn)
30
15
10 10

Use
Domestic Domestic and stock Domestic Domestic and stock Domestic and stock Domestic and stock Domestic Domestic Domestic
Domestic and stock Domestic Domestic and stock Domestic and stock

Remarks some iron

GEORGIA DEPARTMENT OF MINES~,MINING, AND GEOLOGY GEOLOGICAL SuRVEY
Johns Mountaon
I

EX p
Pennsylvanian rocks undivtded
Includes Gizzard Formotton at bose and Sewanee Conglomerate above
Bangor Limestone
~
Floyd She I e Mfs-Fioyd Shale undifferentiated
Mh-Hortselle Sandstone Member at or near top MI-Limestone unit at bose

LA N z

H <f>

w "-
z

::> 0 0w : u.

<(
a:
"-

z
0 DO

<f>

0:

(/}_

<(

<f>

(_)

<f>

~

z

Chert of Mississippian and Devonian age

<(

MOc-Mississ1ppion and Devonian chert undifferentiated
Mfp- Fort Payne Chert Mls-Lovender Shale Member

z 0w>
0

Do-Armuchee Chert

z

<(

il'

Red Mountain Formation

3

EJ

<f>

Upper and Middle Ordovicton undivided

Includes Murfreesboro, Ridley, Moccosin 1 and Boys Formations

z
<(

~

(_)
>

Newolo Limestone

0 0

0:

0

Attalla Conglomerate
~

Knox Group

Ok-Knox Group und1vided, includes Longview Limestone, Chepultepec Dolomite, and Copper R1dge Dolomite
cr-Copper R1dge Dolom1tei approximately the lower half of the Knox Group

I:::'CcsJ.\
cis
f ; ' CS ) '

Western belt

Eastern

z

Conasauga Formation

<(

cl- L1 me stone outcrop

0:

cs i -Mostly shale and some Ccd- Dolomite

DO
:>

l1mestone

Cc-Shole and limestone

<(

(_)

cis-Mostly limestone and

m1xed

some shale

cs- Mostly shale

cs-Siliceous sha le and

thin-bedded sandstone

Rome Format i on

A T

0 N

Contact Long-dashed where approximately
located; short dashed where inferred; dotted where concealed
---10-- -u--
Fault Dashed where approximately locatedi
dotted where concealed U, upthrown side; 0, downthrown side. T, upper plate
--+-Anticltne ApprOJ.imotely located. Shows crestl1ne and dtrection of plunge
--+--
Asymmetric anticline Approxtmotely located Shows cestltne
and direction of plunge. Shalf arrow indicates steeper limb
+-----1 ----
Syncline Apprmcimotely located Shows troughltne
and direction of plunge
Sfnke ond dip of beds
..p!'
Str1ke and dip of overturned beds

Well and number
52 o--
Spring and number

\>
Co
22 C)

Shady Dolomite

0 .<..

.<..

"'
~

(J

QUARRIES
~.h
..Shale ~ Lmestone
~,
Chert
~,
Dolomite
~b Bauxtte
~,. Iron

,.

"'

'

4LL I ~Ll

-

'
~j
-- 3KK _____ /

~

)

' o'

I
) 5KK

L_l

1/

( '2'l0 '

2JJ_) 3JJ

4JJ

5JJ'

~-

I

' '
2\HH

3HH

5H~' '
4HH

' \

0
I

L_ _ _ __I --c__ r--_J

2GG

3GG

4GG

5GG

WELL-LOCATION INDEX

__ ,,.,

15'

\
\

l?
l?
CP
0 0
c
z
-1
-<

WALKER

COUNTY

INFORMATION CIRCULAR 39 FIGURE 4

Srm Cl 0
0 0
z

0

>-
z
0
u
15'
s:
0
1--
n:
<!
ro

\ I I
\ 8

85D22' 30"

p 0 LK

Roc~y
Mounlo n
I

Prepared in cooperation wtth the U. S. Geological Survey, Water Resources Division
i::r:EJ::EJ::EJ::EiDE====c===='E=====3l MILES

COUNTY

Map

of

Floyd

Comty Georgia showing

1

1

geology

and

locations

of wells

and

spr1ngs.

LI ___ _
8'

GEORGIA DEPARTMENT OF MINES, MINING, AND GEOLOGY GEOLOGICAL SURVEY

\

I

I

\

F L 0 YD

~~----

COUNTY

0
c

.---Dim
_ _ j' -;:

()
r
"'
OJ
c
z
"' \ I I
0
c z

-<
Bose mop from County H1ghway Mop, State H1ghway Department

I

\ 85"22"30"

s H A R A L

0 N

I
I

F L0Y D 15'
I
'' - ---''------"' - ___,.j

COUNTY

I
I
d

BARTOW

COUNTY

I
I
I
I

INFORMATION CIRCULAR 39 FIGURE 5

EXPLANATION
(/)

~~~a
Floyd Shale

11}1

1 Ul I-

CaD:

' ::!' <[ u

Sandstone and chert undifferentiated

MDsc -Fort Payne Chert, Frog Mountain Sand- z

stone, and Armuchee Chert, undivided

<!

Mfp- Fort Payne Chert

z

Dim-Frog Mounta in Sandstone, locally inc Iudes some Armuchee Chert. On Indian Mountain probably includes shale

0w>
0

and sandstone ol Mississipp 1on age at top

Do-Armuchee Chert

c 0 u N Ty
Prepared in cooperation with the U.S. Geological Survey, Water Resources Division

tu
PAULDING

tu

I

.>..

I ,__ "'-0>

I 0 ()

I

1'
Strike and dip ot beds
Strike ol vertical beds

Strike and dip ol cleavage
'0
Well and number
52
()-
Spring ond number
QUARRIES
~,.
I ron
~.
Slate
~,
Dolomite
~"
Limestone ~'
Chert
~"
Cloy

,-

2GG

3GG

\

I

-----[__ 4GG

--c__
5GG

2FF\

3FF

4FF

5FIF- 6FF

~_j__- _r_- -~~_ jt_ ~_-_J__ ~ c______ ::::::::_-___l___

J __ _

, . , . , . ,..

WELL-LOCATION INDEX

Rockmart Slate

Drs-Sandstone, conglomerate, and slate in

upper port

z

Or-Slate and siltstone

<[

0

Lenoir Limestone Od-Deoton Member
Newolo Limestone
I a~ I

>
0

u

0

0::

0

0

N
0

w

...J

<[

(l_

Knox Group undivided

Includes Copper Ridge Dolomite, Chepultepec Dolomite, and Longview Limestone

~

z

Conasauga Format ion

<[

cd- Dolomite

0::
(D

-Be-Shale and limestone mixed

:;;

<[

0

Rome Formation

Shady Dolomite METASED IMENTARY ROCKS

To II odego Slate, und iflerent ioted
Includes rocks ol probable Paleozoic age
---------------- Contact
Long-dashed where approximately located; shortdashed where interred; dotted where concealed
-40- - -:r ---?---
Fault
Long-dashed where approximately located; dotted where concealed; queried where doubtful. U,
- - - - + - - - up thrown side; D, downthrown side. T, upper plate Anticline
Approximately located. Shows crestline and direction
ot - plunge - - - + - - Asymmetric anticline Approximately located. Shows crestline and direction
+ - - - - + - - - ot plunge. Short arrow indicates steeper limb Syncline Approximately located. Shows troughline and
direction ol plunge l
-+-- - --~- - - - - --
Asymmetric syncline
Approximately located. Shows troughline and direction ol plunge. Short arrow indicates steeper limb

Map of Polk County, Georgia, showing geo ogy and locations of wells and spn' ngs.