HYDROGEOLOGY OF THE CLAYTON AND CLAIBORNE AQUIFERS IN SOUTHWESTERN GEORGIA by Stephen S. McFadden and P. Dennis Perriello Department of Natural Resources Environmental Protection Division Georgia Geologic Survey 5 5 INFORMATION CIRCULAR For convenience in selecting our reports from your bookshelves, they are color-keyed across the spine by subject as follows: Red Dk. Purple Maroon Lt. Green Lt. Blue Dk. Green Olive Dk. Blue Yellow Dk. Orange Brown Black Dk. Brown Valley and Ridge mapping and structural geology Piedmont and Blue Ridge mapping and structural geology Coastal Plain mapping and stratigraphy Paleontology Coastal Zone stu dies Geochemical and geophyscial studies Economic geology Mining directory Hydrology Environmental studies Engineering studies Bibliographies and lists of publications Petroleum and natural gas Field trip guidebooks Collections of papers Colors have been selected at random and will be augmented as new subjects are published. Publications Editor: Eleanore Morrow The Department of Natural Resources is an Equal Opportunity employer and employs without regard to race or color, sex, religion, and national origin. COVER PHOTO: Center pivot irrigation system in Randolph County, Georgia. HYDROGEOLOGY OF THE CLAYTON AND CLAIBORNE AQUIFERS IN SOUTHWESTERN GEORGIA by Stephen S, McFadden and P, Dennis Perrlel lo Information Circular 55 Prepared os part of the Accelerated Ground~Woter Program GEORGIA DEPARTMENT OF NATURAL RESOURCES Joe D, Tenner, Commissioner ENVIRONMENTAL PROTECTION DIVISION J. Leonerd Ledbetter, Director GEORGIA GEOLOGIC SURVEY WI I Item H. Mclemore, State Geologist ATLANTA 1983 TABLE OF CONTENTS Abstract Introduction Scope of Study. Previous Investigations Acknowledgements. Geography of the Study Area. Location and Demography Physiography and Drainage Climate Geology. Stratigraphy. Providence Sand and Providence Sand Equivalent Clayton Formation. Wilcox Group Claiborne Group. Ocala Limestone. Structure Aquifers In the study area Cretaceous Aquifers Clayton Aquifer Claiborne Aquifer Principal Artesian Aquifer. Ground-Water Use General Clayton Aquifer Claiborne Aquifer Wei I Construction In the Study Area Ground-Water Qual lty Clayton Aquifer Claiborne Aquifer Potentiometric Trends. General Long-Term Potentiometric Trends Clayton Aquifer. Claiborne Aquifer. Short-Term Potentiometric Fluctuations. Clayton Aquifer. Claiborne Aquifer. Ground-Water Ava I labl I lty. General Clayton Aquifer Hydraulic Properties Recharge Analysis of ground-water aval labll lty. Claiborne Aquifer Hydraul lc Properties Recharge An a Iy s I s of ground-water a v a I I a b I I I t y I II PAGE 2 2 3 3 3 4 4 4 4 7 7 7 7 7 8 8 8 8 12 12 12 17 19 19 20 20 22 22 22 22 22 24 30 30 35 36 36 37 37 37 39 39 39 41 41 TABLE OF CONTENTS (Cont 'd): Summary and Recommendations. Clayton Aquifer. Claiborne Aquifer. Recommendations. References Appendices Wei I Location, Construction, and Water-level Appendix A Clayton Aquifer, 1950-1959. Appendix B Claiborne Aquifer, 1950-1959. Appendix C Clayton Aquifer, 1979-1982. Appendix 0 Claiborne Aquifer, 1979-1982. Data PAGE 42 42 42 42 43 46 47 48-49 50-54 55-59 I v ILLUSTRATIONS Plate 1. Geologic Sections of the Clayton Aquifer 2. Geologic Sections of the Claiborne Aquifer ~ (Plates are In Pocket) Figure 1. Location of the Study Area 3 2. Population Growth of Albany and Dawson, 1920-1980. 3 3. Physiographic Districts and Stre8ms of Southwest Georgia 4 4. Ralnfal I Departure Curves -Cities In Study Area 5 5. Structure Contour Map of the Top of the Clayton Aquifer 9 6. Isopach Map of the C I ayton AquIfer 10 7. Structure Contour Map of the Base of the Clayton Aquifer 11 8. Structure Contour Map of the Top of the Claiborne Aquifer 13 9. Isopach M8p of the Claiborne Aquifer 14 10. Structure Contour Map of the Base of the Claiborne Aquifer 1 5 11. Irrigation Trends In Georgia and the Study Area. 16 12. Ground-Water Use In the Study Area 17 13. Typical Wei I Construction In the Study Area. 20 14. Water Quality In the Clayton Aquifer 21 15. Water Quality In the Claiborne Aquifer. 23 16. Potentiometric Surface of the Clayton Aquifer, 1950- 1959. 25 17. Potentiometric Surface of the Clayton Aquifer, December, 1979. 26 18. Potentiometric Surface of the Clayton Aquifer, October-November, 1981. 27 19. Potentiometric Surface of the Clayton Aquifer, March, 1982 28 20. Long-Term Hydrographs of Clayton Aquifer Wells 29 21. Potentiometric Surface of the Cl8lborne Aquifer, 1950-1959 31 22. Potentiometric Surface of the Claiborne Aquifer, December, 1979. 32 23. Potentiometric Surface of the Claiborne Aquifer, October-November, 1981. 33 24. Potentiometric Surface of the Claiborne Aquifer, March, 1982. 34 25. Hydrographs of Clayton Aquifer Wells 35 26. Hydrographs of Claiborne Aquifer Wei Is 36 27. Transmissivity of the Clayton Aquifer. 38 28. Tr8nsmlsslvlty of the Claiborne Aquifer. 40 Table 1. Stratigraphic Column of the Study Area 6 2. Water Use from the Clayton and Claiborne Aquifers. 18 v FACTORS FOR CONVERTING INCH-POUND UNITS TO METRIC (51) UNITS MULTIPLY Inch ( I n ) foot ( f t) mile ( mI ) square mile (ml 2 > ge I I on per minute (gpm) mI I I I on gallons per day (Mgal/d) BY 2. 54 0.3048 1. 609 2.589 0.06309 0.04381 foot squared per day (ft 2 /d) 0.0929 TO OBTAIN centimeter (em) meter ( m) k I Iometer ( km) square k I Iometer (km 2 > I Iter per second (L/s) cubic meters per second ( m3 /s ) meter squared per day < m2 I d > vi ABSTRACT The Clayton and Claiborne aquifers of southwestern Georg Ia are Ioca I Iy Important sources of ground water In a fifteen-county study area. With the exception of the Dougherty Plain district, these aquifers are more productive than the Principal Artesian Aquifer and are the major sources of municipal, Industrial, agricultural, and domestic water for the area. ComparIson of hIstorIc and recent waterlevel measurements Indicates declines of hydrau11 c head In the CIayton aquIfer. Our Ing the period from 1885 to 1981, the hydraulic head In the city of Albany declined approximately 170 teet. Potentiometric maps of the Clayton aquifer show that a cone of depress Ion centered at Albany existed as early as the 1950 1s. As of March, 1982, this cone had deepened and Its radius of Influence had spread Into neighboring counties. Records from throughout the area show that the dec II nes In hydrau II c head are wIdespread, and hydrographs Indicate that the rate of decline has Increased In recent years. Reasons for the dec II ne are Increased mun Ic Ipa I, Industrial, and agricultural withdrawals; limited recharge; and the time-Independent hydraulic propertIes of the aquIfer. Growth In agr Icu 1tural usage has been especially rapid with the number of Irrigation wells In the study area more than doubling since 1977. Total water use from the Clayton aquifer Is estimated to be 26 Mgal/d whl le recharge from rainfall Infiltration averages about 14.7 Mgal/d. The area over which the hydraulic properties of the Clayton aquifer are conducive to the construction of high-yieldIng wells Is relatively small. Because of these factors, the declining potentiometric levels In the Clayton aquifer can be expected to continue. Problems associated with these declines can also be expected to continue or worsen. Measurements of water levels In Ctal borne aquifer wells Indicate that some localized declines In hydraulic head have occurred. A cone of depression Is present around the city of Albany, where the hydraulic head has declined 70 feet from the 1950 1s to 1981. Lesser declines have occurred In the vicinity of the city of Cordele. Declines In this aquifer are due mostly to local municipal, Industrial, and agrlcu ltura I wlthdraw Is, coup led wlth the hydrau lie propertIes of the aquIfer. Recharge to the Claiborne aquifer Is greater and more uniformly distributed than recharge 'to the Clayton aqu Jfer. Tota I water use from the CIa I borne aquifer Is estimated to be 36 Mgal/d while recharge from rainfall Infiltration Is estimated to average 100-133 Mgal/d. Hydraulic properties of the aquifer are such that large withdrawals concentrated In relatively small areas can cause large declines In the potentiometric surface. Although potentiometric declines have as yet not been widespread, the rate of decline and area affected are Increasing. Such declines In areas where the Claiborne aquifer crops out along streams could cause reduced base flow In streams. No single aquifer In the study area Is capable of producing the water necessary to meet current and future demands. In order to reduce continued potentiometric dec II nes and the problems associated with them, particularly In the Clayton aquifer, It Is recommended that future high-yielding wells In the area be of multlaqulfer design and that concentrations of wells producing from a single aquifer be avoided. INTRODUCTION SCOPE OF STUDY This Investigation of the Clayton and Claiborne aquifers In southwestern Georgia Is a part of the Governor's Accelerated Ground-water Program. In the late 1970's, water-level declines as a result of Increased municipal, Industrial, and agricultural ground-water use prompted this study. A survey of available data IndIcated ttie need for an organ Ized and comprehensive study of water-level trends, groundwater quality, ground-water use, aquIfer geometry, lithologic and hydrologic characteristics, recharge and dlscharge mechanIsms, and groundwater budgets. The goa Is of the study were to ass ImII ate existing knowledge, to produce new hydrogeologic data, to Interpret water-level trends In the Clayton and Claiborne aquifers, and to present these data In a usef u I format. PrIor to thIs study, Information on these aquifers was limited and scattered In various fl les and publications. Unpublished data were obtained from flies of the Georgia Geologic Survey (GGS>; Georgia Environmenta I Protection DIvis Ion (EPD); GeorgIa Game and Fish Division; Georgia Parks, Recreation, and Historic Sites Division; u.s. Geological Survey (U. S.G. S.); U.S. So I I Conser vat I on Service; Georgia Cooperative Extension Service; and rrunlclpal governments. Additional Information was obtained from the fl les of well drl tIers, consulting engineers, farmers, Industries, and domestic-well owners. HIs tor I ca I water-1 eve I data were obtaI ned from fl les of the u.s.G.s., GGS, and other flies. Maps of the potentiometric surfaces of the C I ayton and CIa I borne aquIfers were constructed using these data. An observation well network consisting of over 100 municipal, Industrial, Irrigation, domestic, and test wells (some of which were constructed especially for this study) was establIshed to!" both the Clayton and CIa I borne aqu I fers. Water-! eve I measurements were made semll!lnnua lly during periods of approximate seasonal potentiometric highs and lows. The test wells were drilled at selected sites In order to continuously monitor Wl!lter-level fluctuations both In areas remote from pumpIng as we II as near areas of large ground-wl!lter withdrawals. The test wells were constructed In order to compute quantitative aquifer characteristics (I.e., transmissivity, storage coefficient, specific capacity, and others>. Test-well cuttings and other GGS well cuttings and cores were examined to define the I Jthology and geometry of the aquifers and confining units. Where aval table, geophysical logs were used In conjunction with lithologic descriptions to estimate the vertical limits of the aquifers. Specific capacity and aquifer test data were used to estimate transmissivity. Existing ground-water chemistry data were collected and analyzed for significant areal trends. Maps showing the distribution of water quality In the Clayton and Claiborne aquifers were prepared. An analysts was made of water use and recharge to the aqu I tars. Water-use data were supplied by the Georgia Geologic Survey's WaterUse Data Col taction Project. Recharge was estimated from flow-net analysis and by rainfall and surface discharge analysts In areas of aquifer outcrop. Water losses and gal ns from Interaquifer leakage, while discussed In this report, were not quantIfIed. Water-use and recharge patterns coupled with a knowledge of the variations In hydraulic properties were used to analyze the ground-water aval lab I I tty from the Clayton and Claiborne aquifers. PREVIOUS INVESTIGATIONS Several reports have discussed ground-water aval lab II tty In the Coasta I Plain of Georgia. Limited hydrogeologic Information and historic water-level measurements of the Clayton and Claiborne t~qulters are Included In reports by McCa lite ( 1908), Stephenson and Veatch ( 1915), and Thomson and others (1956). Owen (1963) t~nd Walt (1963t~) publ Jshed datal led geologic and ground-water studies of Lee and Sumter, and Dougherty Counties, respectively. These reports Include historic water-level and stratigraphic data. Walt (1958, 1960t~, 1960b, 1960c) also brIef Iy descrIbed the ground-water resources of Clay, Calhoun, Crisp, and Terrell Counties. A separate report by Walt (1960d) discussed the source and quality of municipal ground-water supplies In southwestern Georgia. Vorhls (1972) contrIbuted In format I on on outcrop gao I ogy and structure of the Tallahatta Formation (Claiborne Group) and C I ayton I Jmestone, composIte water levels, and general hydrologic characteristics of aquifers In Crisp, Lee, Dooly, and Sumter Counties. Stewart (1973) discussed aquifer characteristics of the Clayton Formation In the Ft. Gaines area, near the Chattahoochee River. More recently, Hicks and others (1981) discussed the Clayton and Claiborne aquifers In the Albany area. In addition to the above ground-water studies, several other reports have advanced the knowledge of the geologic framework In southwest Georgia. Geologic and paleontologic Jogging by Herrick (1961) establIshed rruch of the baseline control for the subsurface stratigraphy of the Coastal Plain. Toulmln and LaMoreaux (1963) described classic exposures of Tertiary rocks along the Chattahoochee River prior to the Impoundment of the WaIter F. George ReservoIr. Recent contributions by MarsalIs and Frlddell (1975), Swann and Poort (1979), Gibson (1980), Cramer and Arden ( 1980), and RIce ( 1980) have added to the understanding of the geologic history of the area. ACKNOWLEDGEMENTS We wou I d II ke to express our thanks to the many Individuals, those representing Industries and municipalities as well as private landowners In the study area, who have helped by supplying Information and allowing access to their wells. Without their Interest and cooperation, this study would not have been possible. The cooper- 2 atlon of county agents, Agricultural Stabili- zation and Conservation employees, and u.s. Soli Conservation Service personnel Is also deeply appreciated. We thank Harry Blanchard, Frank Boucher, John s. Clarke, Robert E. Faye, and David W. Hicks of the u.s. Geological Survey. Mr. Blanchard was very helpful with historical records, water-level measurement techniques, and water- Ieve I recorder operatIons. Mr. Boucher assisted In pump tests of the wei Is drilled tor this project. Mr. Clarke and Mr. Faye shared va Iuab Ie data and know Iedge of the study area and Mr. Clarke's review of this report resulted In numerous Improvements. Mr. Hicks loaned equipment to our field efforts and also shared Important data and knowledge of the Clayton and Claiborne aquifers In the Albany area. Without the he Ip of these peop Ie, comp Iet Ion of thIs study would have been more difficult. GEOGRAPHY OF THE STUDY AREA LOCATION AND DEMOGRAPHY Figure 1 shows the 15-county area In south- western GeorgIa Inc Iuded In the study. These counties are: Calhoun, Clay, Crisp, Dooly, Dougherty, Early, Lee, Macon, Quitman, Randolph, Sch Iey, Stewart, Sumter, Terre II, and Webster. In this area, the Clayton and Claiborne aquifers are used tor municipal, Industrial, and agricultural water supplies. The population of the area was about 245,000 In 1980 cu.s. Bureau of Census, 1981). AIbany, AmerIcus, and Corde Ie are the only cities with populations greater than 10,000. AI bany (popu latlon 78,000) Is the largest city In the study area and the commercia I center of southwestern Georgia. The city of Dawson (popu latlon 5, 700) Is the center of much of the agricultural activity In the area. Flgure 2 Illustrates the popu latlon growth of Albany and Dawson from 1920 to 1980. During this time period, the population of Albany Increased over 6 times, whl le the population of Dawson remained relatively stable. PHYSIOGRAPHY AND DRAINAGE Most of the study area lies within the Dougherty Plain and Fall Line Hills Districts of the Coastal Plain Physiographic Province (Fig. 3). The Fall Line Hills District Is highly dissected by stream erosion. Relief ranges from 50 to 250 ft, with lower values occurring In the south and southeastern areas adjacent to the Dougherty PI a In. The Dougherty P Ia In DIstrIct 0 50 100 miles Figure 1. Location of the Study Area 80 10 "l ;1;+6 ~ +4 ~ :5 +2 Ill o 1'I -2 \ : \ :~ 1 \ / -4 +16.38 -6 V\ /1 v ' r n ~' " 11 1 1 ,I ~ '- /\ J ~ !~ 1 \ 1\ H . 11 NR ' 0 U1 ci ... +6 aCll a: +4 :S- +2 ::;; Of -2 -4 -6 \A 1\ +8.47 ,1 \ /\{\ l \ /~ r, A 1 \j ~ ! 1r:\}\ f !Y'\ I NR -2.64 -9.16 +6.34 -6.63 NR , I ... ",;' "'Cll +6 z w >~ - o l1l rj . ~r \ , .... J 1 z<( Ill -2 <...(J -4 -6 +5.41 J \ ', , V \,r11, I J \, rI.\t l tI ," \ /1 J \ I I l I \ JI I L \ I I 1\ fitlltrii\Jir tl \ 1 1 r" I I~J rllilll NR +1.83 -2.25 +5.44 -2.77 -3.30 1975 1977 1981 0> 0 o+6 "' i5+4 Cll 3<(: +2 0 0 -2 -4 -6 Figure 4. Rainfall Departure Curves- Cities In Study Area. Plotted are the monthly rainfall departures from the 30-year norm. Annual departures are shown below the curve for each city. \ +14.93 NR ' 1975 1\ -2.58 +3.63 -Q.85 -4.52 NR I 1981 The 30-year norm Is shown next to the city name. All numbers are In Inches. Data from the National Oceanic and Atmospheric Administration. Table I. Stratigraphic Column of the Study Area. SYSTEM EPOCH RADIOMETRIC /SERIES AGE(M.Y.)/STAGE GROUP and FORMATION 25.0 TERTIARY Oligocene Chickasawhayan 33.0 Vicksburgian 38.0 Eocene Jacksonian 41 .0 Claibornian 50.0 55.0 Sabinian 58.0 Paleocene Midwayan 67.0 72.0 Navarroan UPPER CRETACEOUS Gulf ian Tayloran +79.0 Austinian +90.0 Eagle Fordian +94.0 (Modified from Huddlestun, 1981) Woodbinian +95.0 Unnamed Oligocene Limestone Ocala Limestone Clinchfield Sand Claiborne Group Lisbon Formation Tallahatta Formation xo. 0::::1 =~0= "0~ Hatchetigbee Formation Tuscahoma Sand Nanafalia Formation Clayton Formation Providence Sand Ripley Formation Cusseta Sand Blufftown Formation Eutaw Formation Tuscaloosa Formation ~ Atkinson Formation 6 Clayton Formation The Clayton Formation of Paleocene age unconformably overlies the Providence Sand. The lithology of the Clayton Formation varies consIderably. It ranges from a white to gray, glauconitic, recrystallized limestone to a gray, calcareous clay In the Porters Creek Clay facies (Huddlestun, personal communication, 1981). The Clayton Formation Is divided Into three lithologic units (Toulmln and LaMoreaux, 1963, p. 394). The lower division of the Clayton Formation consists of a base I conglomerate and overlying beds of firm calcareous sand and sandstone. The middle division of the Clayton Formation Is a coqulnold limestone containing abundant mollusk shells and bryozoans. The upper division Is a grayish-yellow to white, silty, mlcrofosslllferous, marine, soft limestone. Although sand may be present locally, the Clayton Formation Is generally sand-starved and consists mainly of limestone and clay. In updlp areas the limestone has weathered to an Iron-rich sandy clay. Deposition on an Irregular surface and post-depositional erosion and solutlonlng have caused the thickness of the Clayton Formation to vary considerably within the study area. Thickness ranges from less than 50 ft In eastern Dooly and Crisp Counties to approximately 450 ft In southern Early and Ml ller Counties. WI Icox Group The Wilcox Group of late Paleocene and early Eocene age consists of the Nanafalia Formation, the Tuscahoma Formation, and the Hatchetlgbee Formation. The Nanafalia Formation Is a massively bedded fine- grained, glauconitic sand and sandy clay. The Tuscahoma Formation consists of a basal quartz sand overlain by olive-gray, thinly bedded, laminated, carbonaceous slit and clay Interbedded with fine quartzose sand . 11 relatl vely Impermeable clay layers In the upper Lisbon Formation and below by the clay-rich Tuscahoma Sand and Nanafa Ita Formation. The aquIfer crops out a tong streams In a band runn lng from southwest to northeast through the central and north-central parts of the study area, and Is locally Influenced by stream flow there. Fl gures 8 through 10 are maps I II ustratlng the geometry of the CIa I borne aquIfer In the study area. Figure 8 Is a structure contour map showing the elevation of the top of the Claiborne aquifer, In feet above or below mean sea level. This contact Is the top of the uppermost saturated, permeable sand In the upper Ta I lahatta Formation or the lower LIs bon Formation as determined by well cuttings, cores, and geophysical logs. The top of the aquifer dips to the southeast at a rate of about 14 tt/ml with a more southerly dip along the Chattahoochee RIver In the western part of the study area. This map can be used to estimate the depth to the top of the CIa I borne aquIfer by subtracting the elevation Indicated by the map with the land surface elevation at a given location. Figure 9, an Isopach map cit the Claiborne aquIfer, shows the thIckness of the aquIfer In feet. The thIckness of the aquIfer genera II y Increases from the outcrop area to the southeast and east of the Flint River In Crisp and. Dooly Counties. Note that the thickness Indicated on this map Is from the top of the uppermost saturated, permeable sand to the bottom of the lowermost saturated, permeable sand in the aquifer e and therefore may not represent actua I per.meab I thickness. FIgure 10 Is a structure contour map show- 1ng the e I evat I on of the base of the C I a I borne aquIfer, In feet above or be Iow mean sea Ieve I. This contact Is the . bottom of the lowermost saturated, permeable sand In the lower Tallahatta Formation or upper Hatchetlgbee Formation as determined by well cuttings, cores, and geophysical logs. The base of the aquifer a I so dIps to the southeast. ThIs map may be used to estimate the maximum depth at which the aquIfer wI II be encountered by su btractl ng the elevation Indicated by the map from the la~d surface elevation at a given location. The relatlon!;hJp of the Claiborne aquifer to the CIa I borne Group and other stratIgraphIc units In the study area Is Illustrated by three geologic sections shown In Plate 2. The southeasterly dip and general southerly thickening are shown. Lithologic descriptions of wells used tor the sections tnd lcate facies changes occurring In the study area. PRINCIPAL ARTESIAN AQUIFER Overlying the Claiborne Group In the southern part of the study area Is the saturated, permeable Ocala Limestone. The Ocala Limestone almost exclusively constitutes the Principal Artesian Aquifer In this area. South of A I bany, thIs aquIfer Is the rna In source of ground water for all purposes. North of Albany, however, It thins and becomes less productive, necessitating the use of the deeper Claiborne and Clayton aquifers tor high-yielding wells. Neverthe I ess, In the southern part of the study area, particularly In Dougherty County, the Principal Arte'stan Aquifer suppl les large quantities of water tor Industry and Irrigation. GROUND-wATER USE GENERAL Ground-water use patterns In southwestern Georg I a have undergone rapId change s I nee the turn of the century and particularly In the last 5 to 10 years. During the early 1900's, munlclpa I I ties were the major ground-water users. By the 1950's, Industrial ground-water use had become significant. The use of ground water tor Irrigation began during the 1960's, but did not become common untl I the late 1970's. The majorIty of Irrigation systems were Installed after 1975. Irrigation systems reduce the risk of crop loss due to drought and significantly Increase crop yields. Several, years of below normal rainfall In the mid-1970's through 1981 combined with development of , affordable Irrigation systems have led to rapid growth In their use. Figure 11 II lustrates this growth. Figure I Ia shows that the pumber of ground-water Irrigation systems In the State Increased from less than 300 wells In 1955 to over 4,000 wells In 1981. FIgure I I b shows the Increase In the number of Irrigation wells In the 39 counties of southwestern Georgia and In the 15-county study area from 1977 through 1981. During this period, the number of Irrigation wells In the study area grew from less th~n ?00 to about 800. Water-use data In this report were supplied by the Georgia Geologic Survey Water-Use Data Collection Project. When the project Is complete, water-use data wll I be catalogued according to type of use (I.e., municipal, Industrial, Irrigation, etc.) as well as being subdivided by 12 0 10 20 30 40 Miles I I I I / / M I L L~ R EXPLANATION -too-- STRUCTURE CONTOUR - Shows altitude of top of aquifer. Datum is mean sea level. Dashed where approximately loca ted.Contour interval 100 feet. AREA OF OUTCROP - Includes Claiborne undiffferentiated, Lisbon, and Tallahatta Formations. -105 WELL - Number represents altitude of top of the Claiborne aquifer. Figure 8. Structure Contour Map of the Top of the Claiborne Aquifer (from McKoy, M.L., and Mack, D.M.,, 1983c>. 13 0 10 20 30 40 Miles L __ _ _ __ L_ __ __ _J--~1----~ Ill! STEWART / DOUGH / M.-f L L E R / MITCHELL ' \ 170 EXPLANATION - 100-- LINE OF EQUAL THICKNESS - Shows thickness of entire aquifer. Dashed where approximately located. Contour interval 100 feet. [] AREA OF OUTCROP - Includes Claiborne undifferentiated, Lisbon, and Tallahatta Formations. 167 WELL - Number represents thickness of aquifer. Figure 9. Isopach Map of the Claiborne Aquifer (from McKoy, M.L., and Mack, D.M., 1983a). 14 0 10 20 30 40 Miles STEWART I / / EXPLANATION - 100-- STRUCTURE CONTOUR - Shows altitude of base of aquifer. Datum is mean sea level. Dashed where approximately located. Contour interval 100 feet. AREA OF OUTCROP - Includes Claiborne undifferentiated, Lisbon, and Tallahatta Formations. 272 WELL - Number represents altitude of base of the Claiborne aquifer. Figure 10. Structure Contour Map of the Base of the Claiborne Aquifer (from McKoy, M.L., and Mack, D.M., 1983bl. 15 both county and water source (aquifer or surface water). Only municipal, Industrial, and lrrlgatl on uses are cons I dared here. Data for domestic and other categories of use are Jacking s lnce few records are kept by State and loca I governments or drillers. Water use by domestic and other categorIes, however, Is est I mated to be small when compared to municipal, Industrial, and Irrigation use. Munlclpa I and Industria I ground-water use data are more accurate because large users (over 100,000 gal/d) In these categorIes are requIred under the Georg I a Ground Water Use Act of 1972 to supp I y quarter I y reports of water use to the Georgi~:~ EPD. Irrigation use, however, was exempted from this act and accurate, current data are not available. Irrigation use tor 1980 was estimated by the Georgia Geologic Survey Water-use Data Collection Project using known acreage under Irrigation and type of crop planted (Pierce and Barber, 1981, 1982). A listing of Irrigation wells Is also available from the Water Use Data Col lectlon Project' This listing Is unavoidably Incomplete; also, It Is sometimes not possible to determine the aquifer used due to Jack of well construction Information. The Irrigation estimates used In this report are, therefore, divided Into two groups: (a) use from wells of known construction and therefore known aquifer utllltzatlon and (b) use from wells of uncertain construction. Use In thIs latter category was est I mated by assumIng that the group of wells of unknown construction utilized the aquifers In the study area In the same ratio as the group of wells of known construction. 4200 4000 3800 - 3600 3400 3200 3000 :3 uJ 2800 3 z ~ ~ag:; 2600 2400 2200 u.. 0 cw r 2000 :1:0; 1800 z:::;) 1600 1400 1200 1000 800 600 n400 200 1965 r-- rr-r-,....------ r- No da la 1975 1976 1977 1978 1979 1980 1981 TIME (Years) 3300 3150 - 3000 2850 2700 D Southwest Georgia Study Area [[[I] r-- 2550 .---- 2400 2250 2100 (f) 1950 --~--'' 1800 u.. 0 1650 cr ~ 1500 z 1350 1200 ,....- ,...--- 1050 900 750 600 450 300 M 150 1977 1978 1979 1980 TIME (Years) r-- 1981 Figure 11. Irrigation Trends In Georgia and the Study Area. a). Number of ground-water Irrigation systems In Georgia, 1955, 19751981. b). Number of ground-water Irrigation systems In southwest Georgia and the study area. (Data from Skinner, R.E., 1977, 1978, 1979, and Harrison, K.A., 1980, 1981). 16 The rrunlclpal, Industrial, end Irrigation water-use data reported here are genera I Iy tor the year 1980. However, where aval table, municipal and Industrial water-use figures were updated with 1981 and 1982 data from the Georgia EPD flies. Figure 12 shows ground-water use In the study area by aquifer, and the municipal, Industrial, and Irrigation withdrawals from the Clayton and Claiborne aquifers. The Clayton and CIa I borne aquIfers supp I y about 50 percent of the ground water used In the study area. Table 2 lists water use from the Clayton and Claiborne aquifers by category of use and by county In the study area. Note that these figures are average dally use and do not reflect the highly seasonal nature of water use, partlcu tar ly for Irrigation. During the spring and summer seasons, dally Irrigation withdrawals are much larger than those shown In Table 2, whl le In the fa I I and winter months they approach zero. Municipal withdrawals, although not as variable as Irrigation withdrawals, are also greatest In summer and lowest In winter. CLAYTON AQUIFER The largest municipal and Industrial with- drawals of ground water from the Clayton aquifer occur In the A I bany area. The popu latlon of Albany had grown to 78,000 In 1980 (Fig. 2). Table 2 shows that 7.69 million gallons per day (Mgal/d) were withdrawn from the Clayton aquifer In Dougherty County, coming almost entirely from Albany's municipal wei Is. Industrial use of the C I ayton aquIfer In Dougherty County was about 0.10 Mgal/d, a figure which Is somewhat misleading because some Industries In Albany use Others (mostly Ocala Ls and Providence Sand) 53% 69.59 mgd GROUND WATER USE BY AQUIFER IN STUDY AREA Municipal Irrigation 61% 15.51 mgd Irrigation 63% 22.73 mgd USE OF CLAYTON AQUIFER USE OF CLAIBORNE AQUIFER Figure 12. Ground'"'l'later Use In the Study Area. Irrigation use Is from 1980 data. Municipal and Industrial use are from 1981-82 data. 17 Table 2. Water Use from the Clayton and Claiborne Aquifers. ifers in th~ Stu Area COUNTY AQUIFER Calhoun Clay Crisp Dooly Dougherty Early Lee Macon Quitman Randolph Schley Stewart Sumter Terrell Webster Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton Claiborne Clayton INDUSTRIA!. IRRIGATION known1 extrapolated2 0 0 1.42 0 0 0 1. 01 0 0.45 o. 12 0 0 0.01 4.99 1.37 0.06 0 1. 71 0.24 0 o. 10 0.24 0 o. 10 3.04 1.22 1.06 0.15 0.14 0 1.42 0 1. 58 0.23 0.33 0.07 0.03 0.47 0 4.53 0 0 0 0 0 0 0 0 0 0 2.43 4.31 0,002 0.24 0.51 1.43 o. 71 1.22 1. 73 0 0 0.41 1. 11 MUNICIPAL 0.03 0.35 0.01 0.71 0.13 9.40 7.69 0.79 0.76 0.10 0.33 0.23 0.79 0.15 'IDTAL 0.03 1. 77 1.02 1.28 6.50 0.06 11.35 8.03 4.36 2.00 0.90 1.42 1. 81 0.40 0.03 0.57 4.86 6.97 0.75 2.14 3.74 o. 15 1.52 St udy Area Claiborne 1.82 14.77 7.96 Totals Clayton 0.13 11.94 3.57 11.51 9.96 36.06 27.60 Use of 0: . Use of Information an file indicates zero consumption in this category and aquifer. No record of aquifer use in this category exists, but use may not be ruled out. 1) Known irrigation figures were calculated assuming that individual system consumption is directly proportional to acres irrigated. 2) These irrigation figures are based on the assumption that the group of wells with unidentified aqtlifers have an identical ratio of Clayton:Claiborne:other aquifer wells as the group of wells with aqt~ifer identification. 18 the city's water. In addition to Albany, other municipal users of the Clayton aquifer Include: Arl lngton, Edison, Leary, and Morgan In Calhoun County; Bluffton and Ft. Gaines In Clay County; Cordele In Crisp County; Blakely In Early County; Cuthbert In Randolph County; Sasser, Parrott, Bronwood, and Dawson In Terrell County; and Weston In Webster County. Total municipal and Industrial use from the Clayton aquifer In the study area was about 10. 1 Mga I /d for the time period reported In Table 2. Irrigation systems using the Clayton aquifer are scattered throughout the study area, but they are most concentrated In northern Ca I houn, southern Clay, northeastern Early, eastern and southern Randolph, southern .Terrell, and southern Lee Counties. Yields from the Clayton aquifer are generally highest In these areas. Table 2 shows the total Irrigation use from the Clayton aquifer was about 15.5 Mgal/d. Because 1980 data were used and ground-water use for Irrigation Is constantly Increasing, this number Is probably less than actual current use. CLAIBORNE AQUIFER The largest municipal and Industrial with- drawals from the Claiborne aquifer also occur In the Albany area. The city of Albany withdrew about 9.4 Mgal/d from the Claiborne aquifer during the period reported. In 1979, the Miller Brewing Company constructed a plant In Albany and received a permit to withdraw 3.0 Mgal/d from their three supply wells. Two of these wells tap only the Claiborne aquifer; the third produces water from both the CI ayton and Claiborne aquifers. The Miller Plant currently (1982) withdraws about 1.5 Mgal/d. A Georgia Pacific Corporation plant located near VIenna In Dooly County Is another Industrial user of the Claiborne aquifer, although Its use has been great I y reduced by conservatIon efforts. The company's permit for 2.5 Mgal/d was dropped by the Georgia EPD because Its withdrawals fell below 100,000 gal/d, an Indication of what effective conservation measures can accomplish. Other municipal users of the Claiborne aquifer Include: Leesburg and Smithville In Lee County; Plains, Lest le, and DeSoto In Sumter County; VIenna In Dooly County; Cordele In Crisp County; and Shellman In Randolph County. Total municipal and Industrial use of the Claiborne aquifer In the study area was about 13.3 Mgal/d. In the past, the high cost of constructing large-capacity, screened wells In the sandy Claiborne aquifer restricted Its use. However, the Claiborne aquifer has been heavl ly developed for Irrigation In areas where yields from the Clayton aquifer are not adequate for Irrigation supply. These areas Include southern Early, eastern Terrell, Sumter, Lee, Crisp, Dooly, and southeastern Macon Counties. Yields from the Claiborne aquifer are especially high In Crisp and Dooly Counties. Total Irrigation use of the CIa I borne aquIfer In the study area was about 22.7 Mgal/d during the period reported In Table 2. WELL CONSTRUCTION IN THE STUDY AREA Typical well construction of Clayton and Claiborne aquifer wells and a multlaqulfer well In the study area are shown In FIgure 13. A1though the CIayton aquIfer Is deeper than the Claiborne aquifer, wei Is tapping the Clayton aquifer may be of simple construction and are generally less costly than Claiborne aquifer wells. Typically, a wei I tapping the Clayton aquifer Is constructed by drilling to the top of the aqulter, Instal ling and grouting casing, and then drl I ling Into the aquifer, leaving the bottom of the well as an open hole. The dense, fractured Clayton limestone usually wll I remain open. After drilling Is completed, the well Is dave I oped to remove dr I II I ng f I u Ids from the we I I and aquIfer. Construction of a Claiborne aquifer well Is more complex because the loose sands of the aquIfer norma II y must be screened to prevent collapse of the well. A typical Claiborne aquifer well Is first drilled to the top of the aquifer and casing Is Installed and grouted. A hole Is then drilled Into the aquifer and screens are Installed opposite water-producing sands, which are best determined from geophyslca I logs. The screened I nterva I may or may not be gravel packed depending on the Intended use of the well. Yields generally will be higher In gravel packed wells. After drilling Is comPI eted the we II Is deve I oped to remove drIll I ng fluids from the well and aquifer. The construction of a Clayton and Claiborne multlaqulfer well also Is shown In Figure 13. The well Is screened In the Claiborne aquifer and completed open-hole In the Clayton aquIfer. Multlaqulfer construction has the advantage of the Increasing well yields whl le reducing the Impact on each aquifer and can, In addition, serve to act as a pol nt of recharge from one aquIfer to the other. Note that only the Clayton and Claiborne aquifers have been con- sidered here. In parts of the study area where 19 PRINCIPAL ARTESIAN AQUIFER CONFINING UNIT CLAIBORNE AQUIFEfl CLAIBORNE AQUIFER WELL CLAYTON AQUIFER WELL MUL TIAQUIFER WELL CONFINING UNIT CLAYTON AQUIFER CONFINING UNIT CRETACOUS AQUIFERS .. .; EXPLANATION Screened Interval Open-.hole Interval Cement Grout [Jill Annular Space bmeayGroarvemla~acnkoet d Figure 13. Typical Well construction In the Study Area. they are viable aquifers, the Principal Artesian and/or Cretaceous aqu I tars a I so may be Inc I uded In multlaqulter wells. In order to make the best use of multlaqulter wells, It Is recommended that these we II s be geophys I ca II y Jogged prIor to comp I et I on so that the we I I can be desIgned to take advantage of the water-bearIng units encountered. The many poss I b I e varIatIons and a I ternatlves to the constructions shown In Figure 13 are beyond the scope of thIs study. DependIng on conditions encountered In drilling and the Intended use of the well, construction may vary consIderably. GROUND-wATER QUALITY CLAYTON AQUIFER Ground water from the C I ayton aquIfer In the study area Is a soft to moderately hard, calcium bicarbonate to sodium-calcium bicarbonate type. The qua llty Is genera Jly very good, and meets all standards established by the Georgia EPD In Its 1977 "Rules for Safe Drinking Water". Figure 14 shows the distribution of total dissolved solids . Leakage has been documented through Idle multlaqulfer wells In the Albany area (Hicks and others, 1981, p. 19-20) and may also occur through the confining unit separating the Clayton aquifer from the Providence Sand aquifer. Feldspathlc basal sands In the Clayton Formation which may be In hydrologic continuity with the limestone aquifer also may be the source of the sodium In water from Clayton aquifer wells (Walt, 1960d, p. 12>. 20 0 10 20 30 40 Miles 0 0 L. Y 162 1146) 146 )126) _____, ______ CRISP 32 _ [ I ~ L E E \., I \ I , l ' 164 ;- - ~ .... :..,_ 1120 illn.L _ _ _ ) "l.J ~ 184 11361 ' I '1 __ _ _L ____ ~OJ~ '--"' r: I---200~_/'~;! 18~ 1 6)!l Oti 164 l t36l ' CALHOUN\ :5 172. .179 I ~ . 0 0 U G H Er T y 199 )16) I ~ I I ~N ~ _ Po~ ~ ~ r -- - ~,..r l!.(__ ___ __ _,_~- - - -, ----- 1... _ 1941.., III ; ---"''--"1.1'- i I I MILLER ; BAKER~ , r-) _,/ M I T C H E L L ,-. ( r' ( ' I ~--------~r-~ EXPLANATION - 2 0 0 - LINE OF EQUAL DISSOLVED SOLIDS CONCENTRATION shows concentration in milligrams per liter dissolved solids. Hardness values are not contoured. ~ AREA OF OUTCROP - Includes Nanafalia, Porters Creek, and Clayton Formations, undifferentiated. 1'4c9aJ WELL - Number represents dissolved-solids concentration. Subscript represents carbonate hardness value. Figure 14. Water Quality In the Clayton Aquifer (from Crews, P.A., 1983c). 21 CLAIBORNE AQUIFER Ground water from the Claiborne aquifer In the study area Is genera I Iy a moderate I y hard to hard calcium bicarbonate type. The quality Is good, meeting the drinking water standards of the Georgia EPO. Figure 15 shows the distri- bution of TDS and carbonate hardness In the Claiborne aquifer. TDS concentrations are generally less than 200 mg/1 and nowhere In the study area exceed 250 mg/ 1. South of the study area, however, the chloride content of the CIa I borne aquIfer Increases and the water Is no I onger of good qua llty. ChlorIdes of 11,900 parts per million (ppm) and TDS of 22,200 ppm have been reported In Thomasville, Thomas County (Walt, 1960d, p. 13>. Calcium bicarbonate water Is not typical of a pure sand aquIfer and, In the case of the CIa I borne aquIfer, has been attrIbuted to co- quina and sandy I lmestone beds lnterlayered with the sands of the Claiborne Group and upper Hatchetlgbee Formation. This atypical chemistry has also been cited as evidence of possible leakage to the Claiborne aquifer from the over- lying Principal Artesian Aquifer (Hicks and others, 1981, p. 13). POTENTIOMETRIC TRENDS GENERAL A potentiometric surface Is the level to which water In a properly constructed well (one which Is tightly cased from the water-bearing zone to the surface) wIll rl se due to hydrau II c head. 1 Contour maps of thIs surface were constructed tor the Clayton and Claiborne aquifers by plotting and contouring water-level measurements from a network of observation wells. Potentiometric maps tor different time periods were constructed to Illustrate long-term trends In the potentiometric surface. The direction of ground-water f Iow genera II y Is per pend I cuI ar to the potentiometric contours, from higher to Hydrau lie head Is the sum of pressure head and elevation head. It Is a measure of the potent! a I energy of a unIt mass of water In an aquifer expressed In terms of length. For a more complete discussion of this term, see Freeze and Cherry, 1979, p. 18-26. I n thIs report, hydrau II c head Is assumed equal to the altitude of the static water surface In wells completed In the Clayton or Claiborne Aquifers. lower heads, and Is lnd I cated by t low arrows on the potentiometric maps. A ground-water divide Is a ridge on the potentiometric surface from which ground water flows In both directions and Is represented on the maps by a patterned line. Ground-water divides often coincide with or roughly parallel surface water divides. The configuration of the potentiometric surface of an aquIfer Is affected by groundwater withdrawals. A cone of depression may develop In the vicinity of pumping wells and Is represented on potentiometric maps by closed contour lines with hatch marks pointing Inward. Water levels are successIvely lower toward the center of the cone, and ground-water flow Is toward the center. When there Is a concentration of pumping wells In an area, a cone of depression may become evident on a regional scale. Water-level changes In aquifers are determined by several Interrelated factors. These Include the hydraulic properties of the aquifer, the recharge to the aquifer, and the discharge from the aquifer. The hydraulic properties of the aquifer, such as transmissivity, storage coefficient, and gradient affect the quantity and rate of groundwater movement through an aquifer. The recharge to an aquifer depends on the hydraulic properties listed above, cl lmate (precipitation, evapotranspiration, and streamflow conditions), Infiltration rate (which depends on outcrop area, slope, and permeability), and relationship to other aquifers (head potential and effectiveness of confining units). Discharge can be eIther natura I (Into su rtace streams or through Intervening confining zones Into other aqu I tars) or art If I cIa I (through wells constructed by man). Discharge also depends on the hydraulic properties of the aquifer, climatic conditions, stream base flow, relationships to other aquifers, and withdrawals from wells. LONG-TERM POTENTIOMETRIC TRENDS C I ayton agu I fer Maps of the potentiometric surface of the C I ayton aquIfer have been constructed for tour tIme per I ods: 1950-1959; December 1979; October-November, 1981; and March, 1982. These maps Illustrate the Impact of development on the Clayton aquifer. 22 0 10 20 30 40 Miles STEWART -1'- -~ ~---~~iifJ I ' 160 (l 3 0) 179 C R I 51' 11391 172(131) A R LY ------J~-~- 1'_ -~ ' MILLER w 183 (1 5 5) EXPLANATION -200- rJl l12d 250 (144) LINE OF EQUAL DISSOLVED-SOLIDS CONCENTRATION Shows concentration in milligrams per liter dissolved solids. Hardness values are not contoured. AREA OF OUTCROP - Includes Claiborne undifferentiated, Lisbon and Tallahatta Formations. WELL - Number represents dissolved-soli,ds concentration. Subscript represents carbonate hardness value. Figure 15. Water Quality In the Claiborne Aquifer (from Crews, P.~. , 1983b). 23 Figure 16 Is a map showing the potentiometric surface of the Clayton aquifer during the period 1950-1959. The Impact of withdrawals can be seen even during this time of comparatively little development. Municipal use of the aquifer was becoming significant and Industrial users were developing the aquifer In Albany and Dawson at thIs tl me. A cone of depress I on had developed around Albany, where the lowest hydraulic head, 92 tt, was measured In 1955 at the VIrginia-carolina Chemical Company well near the center of the cone. CI ayton aquIfer we II s In the Albany area which were tree-flowing In the late 1800's and early 1900's, with hydraulic heads up to 220 tt, had stopped t lowIng by the 1950's. The hydraulic head In the city of Dawson was 225 tt, compared with 324 ft In the early 1900 1s. Contours Indicate two groundwater divides which generally coincide with surface water divides. Along the westernmost ground-water divide, flow was to the southwest toward the Chattahoochee RIver and to the south toward MIller County. The other ground-water divide separated water moving to the southw.est from water moving to the southeast toward Dougherty County. F lgure 17 Is a map of the potentiometric surface of the Clayton aquifer In December, 1979. This map shows the heavy Impact of development on the aqul fer. In addition to Increased municipal and Industrial withdrawals, agricultural withdrawals had become significant by 1979. The cone of depress I on at A I bany had deepened and Its radius of Influence had spread to severa I nearby counties. The cone Is elongated toward the northwest In part because of heavy agricultural withdrawals In Calhoun, Randolph, Terrel I, and Lee Counties. The lowest measured hydraulic head was 57 tt at the VIrginia-carolina Chemical Company well In Albany. The hydraulic head In Dawson had dropped to 155 ft. Reductions In the elevation of the potentiometric surface were significant throughout most of the study area, except In areas of outcrop and stream control. Figure 18 Is a map showing the potentiometric surface of the Clayton aquifer In October-November, 1981. Hydrau II c heads measured at thIs tl me were the lowest encountered to date. The tall of 1981 followed a winter of below normal rainfall (see Fig. 4) and a dry summer during which Irrigation withdrawals probably were greater than any previously. The Albany cone of depression had extended northwest and merged with a smaller cone around Dawson. The lowest measured hydraulic head, 37 tt, was measured at the center of the Albany cone, whl le In Dawson the hydraulic head had declined to 125 ft. Figure 19 Is the most recent potentiometric map of the C I ayton aquIfer and was constructed from measurements taken In March, 1982. Compared to the October~ovember, 1981 map, sIgn Itlcant Increases In hydraulic heads were encountered. Most of thIs Increase can be traced to the highly seasonal nature of withdrawals. In an area of high lrrl gatlon use, the potentiometric surface of the aquifer will rebound when pumps are shut ott at the end of the Irrigation season. In addition, rainfall during the winter of 1981-82 was slightly above normal following several years of comparative drought and the water-level rise may, In some areas, ret lect an Increase In recharge from this rainfall. The hydrau II c head at the center of the A I bany cone of depress I on was 50 tt, wh II e In Dawson It was 148 ft. Long-term hydrographs aI so serve to Ill us- trate the changes In water levels In the Clayton aquifer. Long-term hydrographs show trends over a per I od of years but do not ref I ect seasona I fluctuations In hydraulic heads. Figure 20 shows three such hydrographs. Figure 20a Is a composite hydrograph of three wells In the city of Dawson for the tl me per I od 1903 to 1981. In 1981, the hydraulic head In Dawson well No. 4 was 125 ft, compared to 324 ft In well No. 1 In 1903. ThIs represents a dec I I ne of 199 ft, an average of 25 tt per decade. FIgure 20b Is a composite hydrograph of two wells In the city of Edison spanning the years from 1910 to 1981. It shows a decline of 100 tt, an average of 14 tt per decade. FIgure 20c Is a hydrograph of the Atlantic Ice and Coal Company well In Albany from 1885 to 1955, after which the well was destroyed. During the period shown, the hydrau11 c head dec I I ned 88 tt, an average of 14 tt per decade. Claiborne aquifer Maps of the potentiometric surface of the Clalbqrne aquifer have been constructed tor tour periods: 1950-1959; December, 1979; OctoberNovember, 1981; and March, 1982. This sequence Illustrates trends In the potentiometric surface. Although withdrawals have caused some 24 84 - ,.,__f ""';~~. 'l, , I ~J es 32 lj,o iMII.! II "'~,.,.... / E A R Ly 0 , /'""" lttlluol 10 20 EXPlANATION 84 30 MILES AREA OF OUTCROP AND STREAM CONTROL- Outcrop includes Clayton and Nanafalia Formations FAULT- Dashed where approximately located. D indicates downthrown side, U indicates upthrown side POTENTIOMETRIC CONTOUR- Shows altitude at which water level would have stood in tightly cased wells.1950- 1959. Dashed where approximately located. Contour interval 50 feet. Arrow indicates direction of ground-water flow . Datum is mean sea level , tttttttuttlttttttttttttlttlttttttlttt!lll GR0UN0-WAT ER DIV IDE e 39 DATA POINT- Numbers correspond to field numbers in Appendix A. Figure 16. Potentiometric Surface of the Clayton Aquifer, 1950-1959 (modified from Rlpy and others, 1981). 25 84' 85' 32 84' L y 0 10 20 30 MI LES r-:- -- .rJ::~~J EXPLANATION '""''! K~ih1z:j AREA OF OUTCROP AND STREAM CONTROl- Outcrop includes Clayton and Nanafalia Formations. I _..Y__ J D Jl + 150- ~': FAUlT- Dashed where approximately located . D indicates downthrown side, U indicates upthrown side. POTENTIOMETRIC CONTOUR-Shows altitude at which water level would have stood in tightly cased wells, December 1979. Dashed where approximately located. Contour interval 25 feet. Arrow indicates direction of ground -water flow. Datum is mean sea level. IIIIIIIIIIIIIIIIIIIIIIIIIIIIIUIIIIIIIIII e84 GROUND-WATER DIVIDE DATA POINT-Numbers correspond to field numbers in Appendix C. Figure 17. Potentiometric Surface of the Clayton Aquifer, December 1979 (modified from Rlpy and others, 1981). 26 s:s 32" 84" 32" 0 10 20 30 MILES .1 --- '""''~ ~ r.~:- t Sitrll'll~ D 1 -+1~0- _j EXPLANATION AREA OF OUTCROP AND STREAM CONTROL- Outcrop includes Clayton and Nanafalia Formations. FAULT Dashed whore approximately located . D indicates downthrown side . U indicates upthrown POTENTIOMETRIC CONTOUR . Shows altitude at which water level would have stood in tightly cased wells. October-November, 1981. Dashed where approximately located . Contour interval 25 feet. Arrqy.~ indicates direction of groundwater flow. Datum is mean sea level. IUPIIIIIIIIO!tll 84 GROUNDWATER DIVIDE DATA POINT Numbers correspond to field numbers in Appendix C. Figure 18. Potentiometric Surface of the Clayton Aquifer, OctoberNovember, 1981. 27 64" 85 32 64 A R LY 0 10 20 30 MILES ___ JJ::;j EXPLANATION '""~~ ~:::<. Composite hydrograph of Dawson City wei Is. b). Composite hydrograph of Edison City wells. c). Hydrograph of Atlantic Ice and Coal Co. well. (Modified from Rlpy and others, 1981 ) 29 local declines, the Cl11lborne aquifer has remained relatively stable throughout most of the study area. Figure 21 Is a map of the potentiometric surface of the CIa I borne aquIfer tor the tl me period 1950-1959, when the aquifer was relatively unaffected by development. Hydraulic heads ranged from approximately 500 tt In the extreme northern section of the study area to 163 tt In Albany. The map shows the Influence of surface streams on the potentiometric surface. The CIa I borne aquIfer crops out a long many streams In the western and northern parts of the study area. Under most streamflow conditions, the aquifer discharges Into these streams. F I gu re 22 Is a map of the potentIometrIc surface of the C 111 I borne aquIfer for December, 1979. Impact on the aquIfer by thIs date had been mostly local. The most prominent change was the cone of depression which had developed around the city of Albany due primarily to municipal withdrawals. Approximately 49 percent of withdrawals from Albany city wells In 1978 w11s from the Claiborne aquifer (Hicks and others, 1981). The hydraulic head In Albany City Well No. 17 was 95 tt In 1979 compared to 163 tt In 1951, a decline of 68ft In 28 years. The only other area of significant decline from the 1950's to 1979 was near the city of Cordele, where the Claiborne aquifer Is used extensively due to low yields from the Clayton aquifer. The hydraulic head In Cordele City Well No.4 WIIS 239 ft In 1979 compared to 266 tt In 1954, a decline rate of II tt per decade. In most other parts of the study area, declines In the Claiborne aquifer were less than 10 tt tor this time period. F lgure 23 Is a map of the potentiometric surface of the CIa I borne aquIfer tor OctoberNovember, 1981. Some of the lowest hydrau II c heads measured to date were recorded In the fall of 1981. The radius of Influence of the cone of depression around Albany had spread Into neighboring counties. In Albany, the hydrau lie head had declined to 95ft; In Cordele It was 238ft. Figure 24 Is the most recent potentiometric map of the CIa I borne aquIfer, constructed from measurements taken In March, 1982. As with the Clayton aquifer, the seasonal nature of withdrawals 11nd Its effect on water levels Is Illustrated. Significant Increases In hydraulic head were observed throughout most of the study area In the March, 1982 measurements. However, the hydraulic he11d In Albany declined slightly to 93 ft. In Cordele the hydr11ullc head was 247 tt, up 9ft from the previous tall. Comparison with earlier potentiometric maps again shows that throughout most of the study area the CIll I borne aquifer has remained relatively st11ble. SHORT-TERM POTENTIOMETRIC FLUCTUATIONS Potentiometric levels In aquifers vary sea- sona II y because of f I uctu11tl ons In recharge and discharge. Munlclplll and agricultural wlthdrllwals are greatest during the dry months of July through October. More th11n 25 continuously operating water-level recorders have been In- stalled on observation wells by the u.s. Geo- logical Survey and the Georgia Geologic Survey to monitor water-level fluctuations In the Clayton and Claiborne aquifers. Although the greatest rainfall amounts occur In spring and early summer months, this Is also a period of h lgh evapotranspiration. This I lmlts the rlllntall aval table tor recharge to aquifers. Winter Is the season when most recharge to the aquifers occurs. Rainfall events are steady and evenly distributed and evapotranspiration r11tes low. Fall Is generally the driest season and &lso tol lows the season of greatest ground-water use. Therefore, potentiometric levels are usually highest In early spring 11nd lowest In tall. Clayton aquifer FIgure 25a Is a hydrograph of an unused municipal well located In Cuthbert, 45 ml northwest of Albany, tor the period 1972 to 1981. This hydrograph reflects both the Increased seasonal fluctuation and the long-term decline In potentiometric levels due to variations In rainfa II and pumpage. Potentiometric lows occur during the dry months of late summer and early fa I I while highs occur during the peak recharge months of winter and e~~rly spring. Since 19~5, the seasona I lows have been be low those of each preceding year while seasonal highs have not returned to former levels. This Is due to D combination of reduced rainfall and Increased wlthdrawa Is, partIcularly for lrr I gatlon, resulting In a net loss In 11qulter storage (see Fig. 4, rainfall departure curve tor Cuthbert>. FIgure 25b Is a hydrograph of a CI ayton aquifer observation well located near the center of the Albany cone of depression. A record low hydrau II c head of 63 ft was observed In August 1981. This hydrograph also shows the Increased seasonal fluctuations and long-term declines. 30 85' 32' 84' 32 ' R LY 0 84' 10 20 30 MILES I I lui I S:.oo..g'lo jI -uD--- ~:. J t-200- EXPLANATION AREA OF OUTCROP AND STREAM CONTROL- Outcrop includes Tallahatta and Lisbon Formations FAULT- Dashed where approximately located . D indicates downthrown side, U indicates upthrown side . POTENTIOMETRIC CONTOUR- Shows altitude at which water level would have stood in tightly cased wells, 1950 1959 . Dashed where approximately located. Contour interval 50 feet . Arrow indicates direction of ground-water flow . Datum is mean sea level. GROUND-WATER DIVIDE 6 DATA POINT Numbers corn!spond to field numbers in Appendix B. Figure 21. Potentiometric Surface of the Claiborne Aquifer, 1950-1959. (Modified from Rlpy and others, 1981). 31 es 32" 84" r--"-, I I ~~ ~ I u L_-1,-... _ / I .. M 'l, J ( _lI __ _ 32 " R Ly 0 10 20 30 MILES EXPLANATION +-- AREA OF OUTCROP AND STREAM CONTROl- Outcrop includes Tallahatta and lisbon Formations. FAUlT- Dashed where approximately located. D indicates down1hrown side, U indicates upthrown side. +200-- POTENTIOMETRIC CONTOUR- Shows altitude at which water level would have stood in tightly cased wells , December,1979, Dashed where appro xim ately located. Contour interval 50 feet. Arrow indicates direction of ground-water flow . Datum is mean sea level 77 DATA POINT-Numbers correspond to field numbers in Appendix D. Figure 22. Potentiometric Surface of the Claiborne Aquifer, December 1979. (Modified from Rlpy and others, 1981). 32 'l. cj ( lI __ _ l I ______ .._.....,... , I I ~~~~~~~~ ~ I I 32" L y 0 84 10 20 30 MILES / JD_m,_m,--"J ~ -- ---1 EXPLANATION Lu,.fe, i [l(~i3 l AREA Of OUTCROP AND STREAM CONTROL- Outcrop includes Tallahatta and Lisbon formations . I1 - - - FAULT Dashed where approximately located. D indicates downthrown side , U indicates upthrown side. u 1 i-200-- POTENTIOMETRIC CONTOUR Shows altitude at which water level would have stood in tightly cased wells. _j October -November. 1981 Dashed where approximately located. Contour interval 50 feet. Arrow indicates direction of ground-water flow. Datum is mean sea level. DATA POINT Numbers correspond to field numbers in Appendix D. Figure 23. Potentiometric Surface of the Claiborne Aquifer, OctoberNovember, 1981. 33 85 32 84' l, cd ~ _lI __ _ ...r-----, I l I ' I I I I 32" 0 10 20 30 MILES EXPLANATION AREA OF OUTCROP AND STREAM CONTROL- Outcrop includes Tallahatta and Lisbon Formations. FAULT - Dashed where approximately located . D indicates downthrown side. U indicates upthrown side . POTENTIOMETRIC CONTOUR - Shows altitude at which water level would have stood in tightly cased wetls . March 1982. Dashed where approximately located . Contour interval 50 feet. Arrow indicates direction of ground -water flow . Datum is mean sea level. se DATA POINT- Numbers correspond to field numbers in Appendix D. Figure 24. Potentiometric Surface of the Claiborne Aquifer, March 1982. 34 LIJ ~ ~ -125 CLAYTON AQUIFER CUTHBERT, GEORGIA ~ -130 g-140 ~ <...Jt - 135 - LIJ cil ...J ~ L..I.JJ <[ w 320 (/) g w 31 5 w -155 ~ 295 I~:: 290 il <[ - 113 t;:j ~ 103 ~ w 93 0 ::J 5 83 f- 73 < LIJ 63 ~ !3 1 19 78 -:1:9:::7::c9::-LI:9::-8::--0::-'-:-1:9::-8::-;I-...J (/) a:: ~ ;&: Figure 25. Hydrogrephs of Clayton Aquifer Wells. e>. City of Cuthbert, Randolph County. b). Turner City, Dougherty u.s. County. (Source of data Geological Survey>. Claiborne agulfer Prior to 1977, water levels In the Clai- borne aquifer were essentially unmonltored. The u.s. Geological Survey now maintains several ob- servation wells In and near Albany. Seasonal f luctuatlons of 10 to 16 tt have been observed wlth In the A I bany cone of depress I on. Fl gure 26e Is a hydrograph of Test Well 2, located east of the Flint River and within the Albany cone of depression. Seasona I lows occur In the dry months of late summer and fe II wh II e season a I h1ghs occur In the early spring. Seasonal fluctuet Ions very from 7 to 16 ft; however, the period ot record ls too short to establish any long-term trends. Figure 26b Is a hydrograph of a Claiborne aquifer wei I located In Kolomokl State Park In Ear I y County. Seasona I f I uctuatlons are 1 to 3 ft although, again, the period of record Is too short to establish any longterm trends. ThIs hydrograph II I ustrates the effect of below- normal rainfall at this site, which Is near the outcrop of the Claiborne aquifer. Recovery of water levels was very slight during the relatively dry winter of 1980-81. Water levels then dropped sharply during the spring and summer of 1981. 35 Uu J ~ a:: ~ -55 0z -60 j g~ -65 UJ ID -70 1- UJ -7 Uu.J. ~ -80 _j w>UJ - 85 __J ffi -90 ti -95 ~ CLAIBORNE AQUIFER USGS T.W. 2 DOUGHERTY CO. '\.._ 1977 1978 1979 1980 t 1981 1982 __J U> J UJ __J <[ UJ 140 >w"' 135 0 II) ct. 130 1UJ 125 Uu.J. ~ 120 u.i 0 :::> 115 :I:;: 110 <[ uUJ 105 ~ a:: 100 ~ a:: UJ i CLAIBORNE AQUIFER Uu J ~ ~ (/) 0 -74 ~ __J KOLOMOKI PARK g~ -7 5 UJ II) 1UJ Uu.J. -76 ~ _j >UJ UJ __J -77 a:: UJ 1- 3i -78 1977 1978 1979 1980 1981 1982 __J >UJ UJ __J ct. UJ 236 eU";J' II) <[ 1UJ 235 Uu.J. ~ u.i 0 234 ~ 5 <[ 233 tJ ~ a:: ::::> C/l 232 a:: UJ !;i 3:' Figure 26. u.s. Hydrographs of Claiborne Aquifer Wells. a). Geological Survey TW 2, located south of Albany, Dougherty County. b). Georgia Geologic Survey test well located In Kolomokl Park, Early County. GROUND-wATER AVAILABILITY GENERAL The ava I I ab I II ty of water from an aquIfer Is dependent on the complex Interaction of many factors Including volume of the aquifer, hydraulic properties, relatlonshl p to overlying and underlying aquifers and surface streams, the amount and distribution of recharge and the amount and distribution of withdrawals. While It Is not possible to evaluate all these relationships In this report, the following sections will discuss some of these relationships and provide some Insight Into the availability of ground water from the Clayton and Claiborne aquifers. The hydrau II c propertIes of aquIfers are quantified In terms of transmissivity and storage coefficient. Transmissivity Is the rate at whIch water wIll move through a unIt wIdth of aquifer under a unit hydraulic gradient. It Is, therefore, an lnd I cat I on of how an aquIfer wIll transmit water and Is commonly expressed In units of teet squared per day (tt2/d). Aquifers with transmissivity values of less than 150 tt2/d are suited only tor domestic or other use not .requiring high yields. Transmissivity v~ I ues of 1500 tt2/d or greater are adequate tor most municipal, Industrial, or agricultural purposes (Johnson, Inc., 1975, p. 102). Storage coefficient Is the volume of water which an aquifer releases from storage per unit surface area of aquifer per unit change In head. It Is, therefore, a measure of the quantity of us,able water stored In an aquifer and Is a dimension- less number. Values of this coefficient vary greatly In nature and range from 10-5 to lo-2 In confined aquifers. There Is no direct relationship between storage coefficient a.nd availability of water from an aquifer. Another usetu I term In discussIng ground- water aval lability Is specific capacity. Speci- fic capacity Is defined as the rate of withdraw- al (volume per unit time) per unit drop In water level In a pumping well. Specific capacity Is therefore a measure of the yield of a pumping well In a given aquifer. Units are commonly gallons per minute per toot of drawdown (gpm/ft). Note that specific capacity Is depen- dent not only on the hydraulic properties of the aquifer but also on the construction of the well. Variations In specific capacity may or may not Indicate changes In the hydrau lie prop- erties of the aquifer. 36 CLAYTON AQUIFER Hydraulic properties The range and dlstrl button of transmissivity and specific capacity within the Clayton aquIfer are shown In FIgure 27. 1 The transmissivity of the Clayton aquifer varies greatly In the study area. Low values (200-600 tt 2/d) occur south of Albany and east of the Flint River In Crisp and Dooly Counties. The yield of the C I ayton aquIfer In tl'lese areas Is too low tor municipal, Industrial, or Irrigation use. High values (5,000-12,000 tt2/d) occur In the relatively small area of central Clay County, central and southern Randolph and Terrell Counties, and southern Lee County. Intermediate values of 1000-5000 f1,2/d are present In the A I bany area west through Ca Umun and northern Early Counties. The areas of greatest use of the aquIfer correspond to areas of In termed late +o high transmlssl vlty. Note that the bound- aries of the areas Indicated In Figure 27 are Indefinite. It Is possible that for an Individual well In any given location, transmlsslvltles and specific capacities may differ from the range gIven. The large range of transmissivity values In the Clayton aquifer Is the result of several factors. Because the Clayton Formation was deposited on an erosional surface and was Itself eroded after deposition, Its thickness varies greatly over relatively short distances. Facies changes also occur In the Clayton Formation. East of the F II nt RIver and south of AI bany the limestone which makes up the aquifer thins and Increases In clay content, greatly reducing transmlsslv,lty. In the northern part of the stu.dy area, the limestone has been partly or completely removed through solution and erosion, leaving a sandy clay residuum which also has a relatively low transmissivity. Only In the The transmlsslvltles within the Clayton and C 1a 1borne aqu I tars gIven In FIgures 27 and 28 were calculated by several different methods, depending on the amount of data available. The accuracy of these methods varIes; a I though due to the Iarge number of variables Involved, It Is not possible to place numerlca I limits on the error. A II methods lnvol ve some error, depending on the degree to which the assumptions of the method are met In nature. The reader may study the references cl ted on FIgures 27 and 28 tor a more complete discussion of the assumptIons and errors of the d I tferent methods used for calculating transmissivity. 37 relatively small area Indicated In Figure 27 as having Intermediate to high (for the Clayton aquifer) transmissivity Is the aquifer suitable for high-yielding wells. Few va I ues of storage coetf I c I ent In the Clayton aquifer have been calculated due to a lack of complete aquifer tests. An aquifer test performed on the Clayton aquifer during con- struction of the Walter F. George Dam near Ft. GaInes resu I ted In ca I cuI ated storage coeff 1clents of 2.5 x 10-3 to 2.8 x 10-5 (Stewart, 1973). At the Georgia Department of Natura I Resources fIsh hatchery west of Dawson, an aquifer test yielded a storage coefficient of 1. 3 x 10-4 One of the test we I Is dr I I I ed for thIs study, I ocated on the C. T. Mart In farm In southeastern Randol ph County, recorded the drawdown produced by a nearby Irrigation well. The calculated storage coefficient from this record was 1.7 x to-4. Recharge Recharge to the Clayton aquifer occurs In the outcrop area by Infiltration of rainfall and by I eakage of ground water Into the C I ayton aquifer from other aquifers In the study area. Recharge due to rainfall Inti ltratlon Is I lmlted for several reasons. The outcrop area of the Clayton aquIfer Is of I lmlted extent. Estimating from a geologic map of the area (Georgia Geologic Survey, 1976) and cross sections , the outcrop area Is only about 70/80 m1 2 Also, the relatively low permeabl llty of the weathered residuum of the C I ayton II mestone coup I ed wIth reI at I ve I y steep s I opes a Iong stream va I I eys where the outcrops occur results In most of the rainfall which Is not evapotransplred leaving the outcrop area as surface runoff. It Is possible that the outcrop areas of adjacent formations, which are confin- Ing units downdlp but are sandy and relatively permeable In the updlp areas, also contribute recharge to the Clayton aquifer. A t low-net analysIs of the CIayton aquIfer was conducted using the 1950's potentiometric map (Fig. 16) and the transmissivity data avail- able for the aquifer (fig. 27). The analysis Indicates that 16.6 Mgal/d flow south out of the outcrop area of the CI ayton aquIfer Into the area of greatest use. About 1.9 Mgal/d of this flows to the Chattahoochee River, leaving only 14.7 Mgal/d effectively recharging the aquifer. The accuracy of a flow-net analysis Is deter- mined by the accuracy of the transmissivity data and the potentiometric map as well as by the assumptions Inherent In the method. (See Bennett, 1962 for a more complete discussion). 84 85 0 5 I II I I I 1 10 I I 20 miles I EXPLANATION E1Z] Generalized Outcrop Area ~ Transmissivity 5000 ft 2/day to 13,000 ft 2/day Specific Capacity greater than 15 gpm/ft ~ Transmissivity 1000 ft 2/day to 5000 It 2/day Specific Capacity 1 gpm/lt to 15 gpm/ft IJIIII] Transmissivity less than 1000 ft 2/day Specific Capacity less than 2 gpm/ft D No data 2500 A B c o Well location Transmissivity in tt 2/day Transmissivity estimated from a specific capacity. (Source: Brown et al. 1963, pg. 337) Transmissivity estimated from a specific capacity using an estimated pumping time of 12 hours. (Sou~ce: Brown et al., 1963 , pg, 337) Transmissivity estimated from Jacob's approximation of the Theis Nonequilibrium Equation (Source: U.S. Department of the Interior, 1977, pg 113) Transmissivity estimated from a pumping test with an observation well using the Theis Nonequilibrium Equation E Transmissivity from Hicks, Krause. and Clarke, 84 1981, pg. 15. Transmissivity from Stewart, 1973, pg 1. Anomalous transmissivity values which may be the result of well construction. Figure 27. Transmissivity of the Clayton Aquifer. 38 Recharge to the Clayton aquIfer may also occur from other aquifers In the study area. Where potentiometric heads of other aquifers are higher than those of the Clayton aquifer, water can move from the other aquifers Into the Clayton aquifer If some pathway exists. This can occur through leaky confining units, Improperly constructed wei Is, or multlaqulfer wells which are not pumping. Potentiometric head relationships are such that leakage to the Clayton aquifer from the Principal Artesian, Claiborne, and Providence Sand aquifers Is poss I b I e. However, the Pr Inc I pa I ArtesIan and Claiborne aquifers are effectively confined from the Clayton aquifer and It Is unlikely that any significant amount of leakage occurs. The confining unit separating the Clayton and Providence Sand aquifers, on the other hand, may permit significant amounts of ground water to move from the Providence Sand Into the Clayton aquifer. As mentioned previously, some water quality data suggest that leakage occurs (page 12>. The amount of this leakage Is not known. Leakage through Idle multlaqulter wells has been documented In the Albany area. Hicks and other~ ( 1981, p. 20) estimated that 1.1 Mgal/d flows from the CIa I borne and Providence Sand aquifers Into the Clayton aquifer through Idle multlaqulter wells In the Albany area. Added to the 14.7 Mgal/d from rainfall Infiltration, the known recharge to the Clayton aquifer Is at least 15.8 Mgal/d. Analysis of ground-water aval lability The area In which the Clayton aquifer Is productive Is relatively small and has been extensively developed tor municipal and Irrigation use. Withdrawals total about 26 Mgal/d, probably a conservative number, whl le known recharge to the aquifer Is only about 15.8 Mgal/d. Although leakage to the Clayton aquifer from the Providence Sand aquifer may be significant, It Is stl II probable that withdrawals from the C I ayton aquIfer exceed recharge. ThIs explains the rapidly declining potentiometric surface In the Clayton aquifer Illustrated by hydrographs and potentiometric maps. The highest concentratIon of wI thdrawa Is from the Clayton Aquifer, the Albany area, Is located at the extreme southeastern edge of the productive area of the aquifer. Albany also Is removed from recharge from the outcrop area because the most dIrect II ne of recharge, through northern Terrell and southern Webster Counties, Is restricted by relatl vely low transmlss I vltles. The elongate cone of depression centered at Albany Is the result not only of Albany's large withdrawals, but of higher transmlsslvltles and large Irrigation withdrawals In the more productive area of the Clayton aquifer to the northwest of A I bany. It Is not possible at this time to predict the future of the Clayton aquifer. Future rainfa II and growth In ground-water use are not known and, as the aquifers In the study area are further developed, potentiometric relationships may change to eIther Increase or decrease the amount of leakage to the Clayton aquifer. However, It Is unlikely that the long-term declines In water levels will cease. Declines In potentiometric levels can be expected to cause problems of reduction In well yields while pumping costs Increase. Users In some areas may find It necessary to reset pumps, Increase the depth of existing wells, or drill new wells. CLAIBORNE AQUIFER Hydraulic properties The range and distribution of transmissivi- ty within the Claiborne aquifer are shown In Figure 28. Ranges of specific capacity also are Indicated. Transmissivity In the Claiborne aquifer Is more evenly distributed than In the Clayton aquifer, although significant variations can be seen. Transmissivity values throughout most of the study area are In the 2000-6000 ft2/d range. In A I bany, the range Is 2800- 6000 tt2 /d. HIghest va I ues occur east of the Flint RIver In Crisp and Dooly Counties, where transmissivity values In excess of 10,000 ft2/d have been calculated. The Claiborne aquifer Is widely used In these two counties to supply municipal and Irrigation wells. For a I arge part of the study area II tt I e or no data are available. Note that the boundaries Indi- cated In Figure 28 are Indefinite. It Is possi- ble that tor an Individual wei I In a given location transmlsslvltles and specific capaci- ties may differ from the range given. The unl form dlstrl button of transmlssl vlty In the CIa I borne aquIfer when compared to the Clayton aquifer Is the result of a more uniform thickness and lithology. The thickness of the CIa I borne aquIfer does not vary as great I y over short distances as that of the Clayton aquifer. East of the Flint River In Crisp and Dooly Coun- ties, the saturated, permeable thickness of sand units within the Claiborne aquifer Increases to over 100ft. Transmissivity and wei I yields In- 39 84" -,,-,_ _f """"'" l i ~' 85 32 A R LY 31" 85" 0 10 I 11 d t , 1 l I 20 Miles EXPLANATION ETI Generalized Outcrop Area ~ Transmissivity 5000 tt 2/day to 15,000 tt 2tday Specific Capacity 15 gpmlft to 50 gpm/ft Transmissivity 2000 tt 2/day to 5000 ft 2/day Specific Capacity 8 gpm/ft to 15 gpm/ft D 1700 Insufficient data t9 give a range in transmissivity Well location Transmissivity in tt 2/day A Transmissivity estimated from a specific capacity. (Source: Brown et al., 1963, pg. 337) B Transmissrvity estimated from a specific capacity using an estimated pumping time of 12 hours. (Source: Brown et al., 1963, pg_ 337) C Transmissivity estimated from Jacob's approximation of the Theis Nonequilibrium Equation, (Source: U.S. Department of the Interior, 1977, pg. 113) D Transmissivity from Sverdrup and Parcel and Associates. Inc. 1979. * Anomalous transmissivity values which may be the result of well construction. 84 Figure 28. Transmissivity of the Claiborne Aquifer. 40 crease In the same area. Throughout most of the study area, It Is possible that properly con- structed wells can be relatively high-yielding (several hundred to 1000-2000 gpm), although large drawdowns are to be expected. The value of storage coefficient In the Claiborne aquifer Is known In only two loca- tions. An aquifer test at the Miller Brewing Company plant In Albany resulted In storage coefficients calculated In the range of 2.84 x 10-4 to 1. 12 X 10-3 (data from Severdrup, Parcel and Associates, 1979). During construction of the Columbia lock and dam on the Chattahoochee River In Early County, an aquifer test resulted In storage coefficients within the range of 4.3 X 10-4 to 9.9 X 10-4 Recharge Recharge to the CIa 1borne aqu 1fer occurs mostly as Infiltration of rainfall In areas of outcrop. The area of outcrop of the CIa 1borne aquifer has been estimated from a geologic map of the area (Georgia Geologic Survey, 1976) and cross sections o. 55 J.F. Hartsfield 57 R.D. McNeil 58 Albert Adams 59 G.B. Howard 60 E.A. Drew 61 W.R. Veatch 62 c. Roy Wade 66 Sumter 69 Sumter 70 Sumter 99 Sumter 104 Sumter 112 Sumter 117 Sumter 123 Sumter 125 Sumter 127 Sumter Dray ton Methvlns Methvlns Americus Americus Methvins Americus AmerIcus Methvins Methvlns 32"00 1 01 11 - 83"57'15" 32"03'00"- 84"01 1 18 11 32"02 1 45 11 - 84"00 1 56 11 32"04'50" - 84"12'26 11 32"05 1 20 11 - 84"10'23" 32"06 1 44 11 - 84"04'09" 32"04 1 17 11 - 84"11'10 11 32"03 1 19 11 - 84"11'33 11 32"01'50 11 - 84"06'44" 32"00 1 58 11 - 84"04'17" 245 314 321 435+5 474 442 434 374 357 325+4 63 Standard Elev. 64 A.L. Cheek 6 5 T. M F u r I ow 66 W.B. Perry 67 Powe I I Farms K.G. KIndred 130 132 135 298 192 310 200 Sumter Sumter Sumter Sumter Sumter Les I I e Les I I e Americus Drayton Smithvlll e E. 31"59'18"31"59'43 11 32"02 1 49 11 32"00 1 06 11 31"59 1 57 11 - 84"01'47" 84"03 1 21" 84"13'23" 83"57 1 24" 84"11'59" 322 31 8 390 245 357 69 Deseret Farm #1 70 s.w. Ga. Exp. 701 Station Sumter Sumter Les I I e Lake Collins 31"56 1 12 11 - 84"00 1 33" 32"02 1 10 11 - 84"22 1 02 11 300 4 98 71 John 0 'Hearn 72 Highland Gate 73 A.P. Lane 207 87 285 Sumter Sumter Terrell Americus Smithville w. Bronwood 32"05 1 37 11 31"59 1 53 11 31"49 1 04" - 84"13'46 11 84"15 1 01" 84"18 144" 458 405 311 74 Steve Cocke Fish 683 Terrell Dawson 31"46 1 21 11 - 84"28 1 54 11 388 Hatchery #2 75 City ot Sasser #1 368 Terre I I Sasser 31"43 1 08 11 - 84"20 1 52" 31 5 103d 220d 86d 65d 63d 75d 132d 64 d 135d 260d 1 84c 160d 1 ODd 93d 107c 12 7d BOd 62d BOd 85d 125d 140d BOd I ODd 85d 179d 88d 105d 111d 12 7c 202c 201d 200d 64c 68e 78c - 59.23d - 40d - 43.4d - 40d - 45d - 49.3d - 14. 7d - 51 d -129.3d - 11.85d + 5. 6d - 29.2d - 28.3d - 63. 9d - 74. 5d - 79. 2 d - 49.2d - 15. 7d - 24d - 18. Bd - 34.2d - 16. 5d - 19. 3d + 7d - 44.6d - 43d - 50d - 69.5d - 35d - 19. fie - 45.6c - 40d 1 950 1952 1 950 1950 1 950 1950 1 951 1950 1 950 1951 1 950 1951 1 951 1 951 1 951 1951 1 951 1951 1 951 1951 1 951 1 951 1 951 1951 1 952 1958 1 958 I 952 1 951 1952 1 954 1955 * Approximate Location: Latitude+ 1' Longitude..:!:_ 5" APPENDIX C -WELL DATA FOR ltjE POTENTIOMETRIC SURFACE OF ltjE CLAYTON AQUIFER (1979-1982) FIELD NO. OWNER GGS GC NO. NO. COUNTY QUAD LAT. - LONG. LAND SURFACE ELEVATION (teet) TOTAL DEPTH (feet) CASING DEP"ftj (teet) STATIC WATER LEVEL (SWL) DATE MEASURED SWL DATE SWL DATE SWL DATE 17 City at Edison 353 #2 Calhoun Edison 3133 134"- 8444'15" 289 515 395 - 103.3 12/79 -104.0 3/81 -121.2 11/81 -104.5 3/82 23 (Speight School) 402 Clay Co. E\em. School 29 w.s. Stuckey 305 164 Clay Dooly Ft. Gaines Unadilla 3136 137 - 85.02'06" 390 3217 103"- 8344 138" 412 500 340 408 373 - 270.3 11/81 -259.6 3/82 - 68.8 4/81 - 93.0 3/82 34 Sw Itt & Co. (VI rgl n la-caro I Ina Cheml ca I Co. J Dougherty Albany w. 3134 148"- 8410'06" 197 594 - 151 3/81 -159.8 10/8: -146.9 3/82 35 Turner City #2 Dougherty Albany E. 3135 153"- 8406 126" 213 760 713 - 134.0 11/79 -123.0 3/81 -146.0 10/81 -127.6 3/82 38 . 3/81 11/81 3/82 143 C.T. Martin 3449 Randolph Doverel 31 "39'53 11 - 84"36'1211 322 430 356 - 126.4 -148.2 -127.0 o.w. #2 3/81 10/81 3/82 144 J lmmy Bangs #2 145 Raymond Goodman Terrell Chlckasawhatchee Webster Benevo I ence 31"38 1 55 11 - 84"29 1 5511 300 31 "57 1 25 11 - 84"38 1 0311 530 500 400 240 - 128.8 12/79 - 141.5 3/81 -137.0 3/81 -157.9 10/81 -144.1 10/81 -130.5 3/82 -132.7 3/82 146 Pete Long o.w. 3517 .#1 147 vtj h;;,rans. Memorial Park TW - I 3518 148 Featherfield Farms Lee Crisp Smithville W. 31"53 1 53 11 - 84"19 1 25" 338 Cobb 31"57 1 31 11 - 83"54 12311 252 Dougherty Holt 31"35 141 11 - $4"26 105 11 228 384 332 550 510 585 485 - 151.8 -133.8 10/81 3/82 - 39.8 4/82 - 78.4 3/82 150 City of Dawson Maintenance 8drn Terrell Dawson 31 "46 1 36 11 - 84"26'13 11 355 - 215.7 3/82 151 Ben Arthur Terrell Bronwood 31"46 1 01 11 - 84"20 132 11 325 543 440 - 177.65 3/82 APPENDIX D-WELL DATA FOR THE POTENTIOMETRIC SURFACE OF THE CLAIBORNE AQUIFER (1979-1982) FIELD NO. OWNER GGS oc NO. NO. COUNTY QUAD LAT. - LONG. LAND STATIC WATER SURFACE TOTAL CASING LEVEL CSWLl ELEVATION DEPTH DEPTH DATE SWL SWL SWL (feet) (feet) (feet) MEASURED DATE DATE DATE 10 City of Cordele 390 14 Crisp Cordele 31"58'16 11 - 8346'2811 316 600 270 - 76.5 12/79 - 76.5 3/81 - 78.5 10/81 - 69.5 3/82 26 City of Albany #17 Dougherty Albany E. 31"35'5511 - 84"06'2611 208 7DO 200 - 113.4 1/80 -114.0 2/81 -115.0 4/82 01 01 32 City of Shellman Randolph Shellman 31"45'31 11 - 84"36'58" 393 135 - 35.5 - 35.5 - 31.5 - 34.5 12 12/79 3/81 10/81 3/82 37 F. \tlaltsman II 282 188 Sumter Americus 32"01'4811 - 84"13'0511 373 129 106 - 51.5 12/79 - 23.1 3/81 - 53.6 10/81 - 51.9 3/82 67 (K.G. Kindred) 310 200 Sumter Smlthvlll e E. 31"59'5711 - 84"11 1 59 357 85 CJ. Deriso) Powell Farms - 43.2 12/79 - 39.9 - 45.5 3/81 10/81 - 40.4 3/82 75 City of Sasser 368 II Terrell Sasser 31"43 108"- 84"20'52" 314 201 181 - 40.0 12/79 - 44.5 3/81 - 46.9 10/81 - 35.3 3/82 77 Great Southern 729 Paper Company Early Gordon 31"09'5211 - 85"05'45 120 380 380 - 21.2 12/79 - 19.5 3/81 - 15.0 11/81 - 22.9 !/82 APPENDIX D - WELL DATA FOR THE POTENTIOMETRIC SURFACE OF THE CLAIBORNE AQUIFER (1979-1982) FIELD NO, OWNER GGS oc NO, NO. COUNTY QUAD LAT. - LONG. LAND SURFACE ELEVATION (feet) TOTAL DEPTH (feet) CASING DEPTH (feet) STATIC WATER LEVEL (SWL l DATE MEASURED SWL DATE SWL DATE SWL DATE 80 SIng Ietary Farms 82 Grady Milliner 83 McNair #I 3151 3388 84 H,T. Mclendon #4 Early Clay Calhoun Calhoun Bancroft Zetto Bluff ton 8 luff ton 31 "25 1 13 11 - 8450'01 11 250 31"32'37 11 - 84"52 1 43 11 355 31"34'35"- 8447'15" 352 31"35 1 00 11 - 84"47 1 2911 365 200 188 150 140 103 140 120 - 42.8 - 43,3 12/79 3/81 - 59.9 - 61.8 12/79 3/81 - 54.6 - 55,2 12/79 3/81 - 71,4 - 69,2 12/79 3/81 - 32,4 11/81 - 15.9 3/82 - 62,1 10/81 - 59,7 3/82 - 56.2 10/81 - 53,0 3/82 - - 70.0 66,8 10/81 3/82 85 Isler Farms Flying Service Clay Zetto 31 "36 1 07 11 - 6452'3911 420 142 80 - 64.3 - 64.6 - 64.2 3/81 10/61 3/82 86 E. Alday (G. Chapman l Clay Bluff ton 3136 1 49 11 - 84"51'3711 405 122 67 - 44.4 - 45.5 - 45,7 - 44,7 12/79 3/61 10/81 3/S2 88 W.D. Beard #I 3366 Calhoun Morgan 31 "34 1 45 11 - 8435 1 0211 254 140 - 14.0 - 16,8 - 16.6 - 11.8 (1'1 11/79 3/61 10/61 3/82 Ol 89 w. Stan Iey Randolph Carnegie 31"43 1 04 11 - 8451'1511 470 50 - 42.8 - 42.7 - 44.3 - 42, I 12/79 3/61 11/81 3/82 90 Gene Kennedy 91 Melvin Peavay 12 Randolph Randolph Cuthbert Brooksv II le 3147'26 11 - 84"47'1011 474 31"45 1 51 11 - 84"39'2311 425 66 50 - 39,0 - 39.3 - 40,3 - 36.0 12/79 3/81 11/81 3/82 110 - 38.6 12/79 92 Dean Whaley #2 Randolph Brooksville 31"45 1 36 11 - 84"39 1 1011 418 110 - 33,8 12!79 94 Dean Whaley #I Randolph Shellman 31"50 1 21 11 - 84"37 1 0911 470 90 60 - 63,9 - 69,6 - 67.7 - 68,2 12/79 3/81 10/81 3/82 95 Bob Chamb I Iss Terrell Dawson 31 "45 1 56 11 - 84"28 1 2311 371 180 - 35,5 12/79 - 37.5 3/81 - 38.9 10/81 - 41,4 3/82 96 Sonny Reese Terrell Chlckasawhatchee 31"41'33 11 - 84"25 1 57 11 270 200 60 - 7.9 - 7.2 - 9,4 - 5,9 12/79 3/81 10/81 3/82 97 T.W. #11 3384 Dougherty Reds tore Crossroads 31 "26 1 54 11 - 84"21'01" 182 320 300 - 22,9 12/79 - 29.0 3/81 - 27,6 10/81 - 27,34 3/82 98 r.w. fl4 Dougherty Pretoria 3135'30 11 - 84"20 1 32 11 220 251 232 - 17,0 12!79 - 22.0 3/81 - 26.3 10/81 - 18,27 S/82 APPENDIX D - WELL DATA FOR THE POTENTIOMETRIC SURFACE OF THE CLAIBORNE AQUIFER (f 979-1982) FIELD NO. OWNER GGS oc NO. NO. COUNTY QUAD LAT. - LONG. LAND SURFACE ELEVATION (teet) TOTAL DEPTH (feet) CASING DEPTH (feet) STATIC WATER LEVEL !SWL) DATE MEASURED SWL DATE SWL DATE SWL DATE 100 T.w. #2 Dougherty AIbany East 31 31'05 11 - 84"06 143 11 195 418 398 - 70.3 12/79 - 88.0 3/81 - 90.4 10/81 - 79.55 3/82 101 T.w. #5 102 o.w. #2 MI II er Brewery Dougherty Albany West Dougherty Albany East 31 "35'34"- 84"10 1 3011 198 31"35'45 11 - 84"04 14711 205 257 237 560 300 - 84.6 12/79 - 66.0 12/79 - 83.0 3/81 - 88.2 10/81 - 79.94 3/82 103 T.w. 18 Lee Leesburg 31"38'13 11 - 84"12 1 5011 238 385 - 97.0 12/79 - 99.0 3/81 -106.7 10/81 - 94.5 3/82 104 W.H. Fryer Lee Sasser 31 "40'08 11 - 84"17'2611 258 263 100 - 37.0 12/79 - 29.5 3/81 - 46.3 10/81 - 32.2 3/82 105 J. Daniels #2 Terrell Sasser 31"41'20 11 - 84"19'0911 290 320 100 - 52.9 3/81 - 54.0 10/81 - 40.9 3/82 107 Sheriff J. Dean Terrell Dawson 31 "47 1 48" - 84"25 1 0511 340 120+5 84 - 23.5 - 24.0 - 26.3 - 19.9 C1l 12/79 3/81 10/81 3/82 -...1 108 Jack Balentine Terrell Parrott 31"54'01 11 - 84"30'1911 450 60 - 34.5 12/79 - 38.4 3/81 - 40.6 10/81 - 40.0 3/82 109 John Wills Terrell Bronwood 31"50 1 26 11 - 84"20'5511 362 120 89 - 51.4 - 49.4 - 52.6 - 44.1 12/79 3/81 10/81 3/82 110 John Wise Terrell Bronwood 31"47 1 08 11 - 84"17'21 301 135 - 39.7 12/79 - 35.5 3/81 - 43.6 10/81 - 31.9 3/82 111 Ha Iey Brothers Farm Lee Leesburg 31"41'13"- 84"13 1 2211 220 300 - 35.9 12/79 - 35.1 3/81 - 57.2 10/81 - 50.4 3/82 113 Gloria Spann Sumter Plains 32'01 '17"- 84"24 109 503 50 40 - 42.3 - 44.2 - 44.5 - 42.5 12/79 3/81 10/81 V82 114 City of Plains #4 Sumter Plains 32"02'09 - 84"23'12 11 491 90 80 - 31.7 3/82 115 Dru or Dave Murray 314 210 Sumter Plains 32"03 1 00" - 84"23'2511 509 86 76 - 50.1 - 49.3 - 51.3 - 52.0 12/79 3/81 10/81 3/82 116 C Ity of P Ia Ins 113 117 S.w. Ga. Exper1- 2157 ment Station #1 Sumter Sumter Plains Lake Collins 32"02'07" - 84"23 1 2011 494 32"02 1 48 11 - 84"22'1611 510 91 80 - 32.5 - 30.2 - 33.9 12/79 3/81 10/81 107 70 - 56.6 - 53.5 - 57.4 - 58.4 12/79 3/81 10/81 3/82 APPENDIX D-WELL DATA FOR THE POTENTIOMETRIC SURFACE OF THE CLAIBORNE AQUIFER (1979-1982) F IELD NO. CJ.oiNER GGS oc 1(). 1(). COUNTY QUAD LAT. - LONG. LAND SURFACE ELEVATION (feet) TOTAL DEPTH (teet) CASING DEPTH (feet) STATIC WATER LEVEL (SWL) DATE ~lEASURED SWL DATE SWL DATE SWL DATE 119 R.S. Moore 296 120 Clark Rainbow 709 Center - PurIna Sumter Sumter Ellavl I le Americus 32"09'14 11 - 84"18'25" 512 32"07'11"- 84"11'4611 461 154 70 136 126 - 67.6 12/79 - 42.2 12!79 - 69.7 3/81 - 41.7 3/81 - 69.5 10/81 - 45.4 10/81 - 68.7 3/82 - 45.4 3/82 123 Henry Hart #lA Sumter Smithvl I leE. 31 "59'37 11 - 84"09'0911 343 90 - 27.3 - 26.6 12/79 3/81 - 36.9 10/81 - 21.5 3/82 124 Charles Miller 3358 Sumter Cobb 31"56'37 11 - 83"58 1 5911 285 310 230 - 26.5 12/79 - 22.6 3/81 - 39.4 10/81 - 17.9 3-'82 125 Ga. Veterans 2252 Mem. State Park Crisp Cobb 31"57'17 11 - 85"54 1 5011 262 300 - 25.5 12/79 - 26.5 3/81 - 28.6 10/81 - 24.8 3/82 126 W.T. Greene Crisp Cordele 3159 1 27 11 - 83"49 1 3811 312 400 200 - 35.4 12/79 - 34.6 3/81 - 37.1 10/81 - 32. I 3/82 128 E.o. Cannon en 00 Dooly Drayton 32"03'28 11 - 83"54 1 0311 310 200 - 39.9 12/79 - 40.4 3/81 - 45.5 10/81 - 37.4 3/82 129 Dr. James 1-llnor Dooly Byromville 32"10 1 17 11 - 83"58 1 33" 325 290 70 - 40.7 - 41.6 - 49.9 - 42.2 12/79 4/81 10/81 3/82 130 HardIgree #1 Dooly VIenna 32"06 1 42 11 - 83"50'4011 340 340 240 - 40.6 l/80 131 City of Vlenn<> 143 #I Doo ly VI anna 32"05 1 39 11 - 8347'31" 355 571 571 - 65.8 12179 - 64.5 3/81 - 67.2 10.81 - 60.5 3/82 132 WI I I lam Sparrow Dooiy Pi nevlew N.w. 32"13'15 11 - 83"42 1 2311 370 280? 175 - 41.0 4/81 - 48.4 10/81 - 37.5 3/82 133 George McKay 1805 Crisp Drayton 32"0120 11 - 83"54'05" 288 170 125 - 25.4 12179 - 26.5 3/81 - 30.4 10/81 - 24.3 3/82 134 Judge Horn Crisp Cobb 31 5910 11 - 83"54'55" 265 300 - 16.1 12/79 135 City of Unadilla #3 Dooly Unadilla 32"15 1 06 11 - 83"44'23 376 315 315 - 57.1 12/79 - 57.2 3/81 - 63.9 10/81 - 53.5 3/82 136 TerrIll Hudson 138 City of Byromville 11 Dooly Dooly Henderson Byromvl lie 32"1527 11 - 83"47 1 2511 430 32"12'14 11 - 83"54 1 29" 380 400 200 203 - 100.3 3/81 - 91.0 4/81 -104.4 10/81 -105.1 10/81 - 97.75 3/82 - 92.7 4/82 APPENDIX D - WELL DATA FOR THE POTENTIOMETRIC SURFACE OF THE CLAIBORNE AQUIFER ( 1979-1982) FIELD NO. OWNER GGS oc NO. NO. COUNTY QUAD LAT. - LONG. LAND SURFACE ELEVATION (feet) TOTAL DEPTH (feet) CASING DEPTH (feet) STATIC WATER LEVEL (SWLl DATE MEASURED SWL DATE SWL DATE SWL DATE 139 Henry Hart 112A Sumter Smithville E. 31 57'54" - 84 08'08" 348 125 - 53.5 10/81 - 33.6 3/82 140 Boots Lyles Sumter Smlthvl I leE. 3158 1 34 11 - 8407'4311 365 300 - 70.4 10/81 - 50.4 3/82 142 John Daniels #1 Terrell Sasser 3141'42"- 8419 134" 309 320 - 34.6 3/82 143 Marcus Regans Randolph B I uffton 3137'17"- 8449'51" 360 124 103 - 45.3 12/79 - 45.2 3/81 - 46.5 11/81 -44.9 3/82 145 Shingler & Reed Early Gordon 3110'15"- 8500'43" 211 460 280 - 85.8 11/81 - 78.3 3/82 (.]1 tO 146 Kolomokl State Early Blakely N. 3128'27- 8455'1511 310 140 120 - 74.8 - 76.9 - 75.4 Park T .w. 113 3/81 11/81 3/82 148 Shiloh Church Terrell Shellman 31"49'35- 84"33'11 11 365 60 - 36.8 12/79 150 HardIgree #2 151 F I rewel I Mi I I er Brewery 154 Clty of Smith- ville #2 2137 Dooly Dougherty Lee V lenna Albany E. Smithville w. 32"06'46- 83"49 1 2311 341 31 36 1 25- 8404'1511 200 3154 1 02 11 - 8415'2911 328 360 300 350 195 195 - 32.1 3/81 - 72.0 3/81 - 36.5 3/81 - 35.5 10/81 -104.5 10/81 - 39.4 10/81 - 28.5 3/82 - 90.63 3/82 - 34.3 3/82 155 C.T. Martin o.w. #1 156 Pete Long o.w. #2 Randolph Lee Doverel Smithvi lie W. 3139 1 53 01 - 8436'12 11 322 3153 1 53"- 8419 1 25 11 338 94 77 143 112 - 29.5 3/81 - 39.2 10/81 - 30.6 10/81 - 36.8 3/82 - 27.4 3/82 159 CIty of Leary 2239 Calhoun Leary 31 29'12 11 - 8430 1 4711 205 556 - 31.7 3/82 ' GEORGIA GEOLOGIC SURVEY GEOLOGIC SECTIONS OF THE CLAYTON AQUIFER From Tuohy, M.A., 1983a A soo' Ill - - - MJ - - SUMTER - - - - - - + - - L E E - + - - - - - - - - - TERRELL 40o' 3001 20o' IOo' 0 -IOo' -20o' .Joo' - 4001 - - - - ----- ClAIBORNE GROUP A' CALHOUN ------- ---------------------t-----------------------EARLY ------------------------ GGS 437 ClAIBORNE GROUP WILCOX GROUP --- - --- INFORMATION CIRCULAR 55 PLATE I A- - - A' GEOLOGIC SECTION e WELL LOCATIO N 20 -40 BO Milu -9o~L-------------------------~~o~----------------------~2~o~----------------------~,o~----------------------~,~6------------------------~sto~-----------------------:6~o------------------------~7o~----------------------~8~0------------------------~9~0~----------------------~~~oo Mil B -t--------------- soo ALABAMA' -HENRY CLAY - - - - - - - + - : G : - : G S : - . - - - - - - - - - - - CALHOUN 11! GGS Ill DOUG HERTY GGS GGS 11 415 B' CR ISP WORTH ---------r-GG~ IDI Mea n Sea Level 0 CLAIBORN E GRou p ClAIBORNE GROUP ---- - - WI LCOX GROUP LIT HOLOG Y EXPLANATION ACCESSORIES D C h e rl c GsGnS WEBSTER soo' 400 1 TERRELL GGS 211 c DOUGH ERTY - - - - - - - llr BAKER+----------------- MITCHELL GGS 101 GGS t1 GGS )101 ~~~~@~~~~~~ Clay . lim estone t ; j Marl CORRELATION CHART ( After Pul Huddle.,tun.11i1B1) I I ~_-- : : Clay streaks 80olomite D Macrofossi l s 8 Interbedded limeston~. c==.J lntorb ed ded marl -3 001 -soo1 - I>Oo' -700' -8 001 -9 001 -10001 -11001 -12001 - 13001 -14 001 ________________________ - 1soo L-------------------------~1oL-------------------------21o _JJoL-------------------------~lo--------------------------soL-------------------------6~o~----------~-----------:,:o-------------------------;,ao M il., r-::-1 Finely disseminated L__j phosphate grains 1- I~- Glauconite MISCEUANEOUS SYMBOLS Clayton aq uif er ~No samplt> - - - - ln dei inile bound ary Cartography by E.S. Ramos GEORGIA GEOLOGIC SURVEY A - - - - S C i t U Y - - - + - - - - - - - SUMTER 11111 Gill GGI 315 296 so GEOLOGIC SECTIONS OF THE CLAIBORNE AQUIFER From Crews, P.A., 1983a A' lEE-----------------+---------------------- DOUGHERTY ---------------------+---------- MITCHEll----------- GGS GGS 261 109 INFORMATION CIRCULAR 55 PLATE 2 Mea n Sea level 0 -4001'--------------L-------------' 10 M il s A -- A' GEOLOGIC SECTION 10 20 30 40 B EARlY ClAY CALHOU N GGS GGS GGS 437 138 353 so RANDOLPH 60 GGS 350 70 TERRELl 80 90 M il., B' SUMTER - - GGS 504 / / / / / / / / / / Clayton fm WILCOX GROUP Clayton fm. l.-------------~~o~------------~2~0~----~-------~3~0~-------------t40~------------~5~0~------------~6~0;-------------------,7~o;-------------------------~~o Mils c RANDOlPH GGS 552 c TERRELL -------+-- LEE --+------------- SUMTER ---------------t---------- DOOLY -------- GGS GGS GGS GGS 352 406 137 143 EXPLANATION LITHOLOGY ACCESSORIES Bchert 8 lnlerbed ded marl ~~~~~~~~~~=d Clay g umeslon e ITT TIMarl I - - I ~ ~ ~ Clay streaks. 0 o o lomite r--:1 L__:__j Finely d issem i~ ated phosphate gra1 ns D Glauconite 8 Ma cro fossi ls Q In terbe dd ed lim w one CORRELATION CHART (After Paul H~o~dd leet un, 1 981) lli milsand MISCELL ANEO US SYMBOlS Claiborne aquifer ~N o samplts - - - - Ind efini te bound ary 0 - 2001 L--------------~.~o~--------------~2~o~-----------------~3~o~-------------------------.~o~------------------------~so~-------------------------;6~o--------------------------~7o Mil Cartograptly by E. S. Ramo s