Geohydrology of the Albany area, Georgia

GEOHYDROLOGY OF THE
ALBANY AREA, GEORGIA
by D. W. Hicks, R. E. Krause, and J. S. Clarke
Prepared in cooperation with the U.S. Geological Survey and the
Albany Water, Gas, and Light Commission
Department of Natural Resources Environmental Protection Division
Georgia Geologic Survey

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57 INFORMATION CIRCULAR

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GEOHYDROLOGY
OF THE ALBANY AREA, GEORGIA
by
D. W. Hicks, R. E. Krause, and J. S. Clarke
Prepared in cooperation with the U.S. Geological Survey and the
Albany Water, Gas, and Light Commission
DEPARTMENT OF NATURAL RESOURCES Joe D. Tanner, Commissioner
ENVIRONMENTAL PROTECTION DIVISION J. Leonard Ledbetter, Director
GEORGIA GEOLOGIC SURVEY William H. McLemore, State Geologist
Atlanta 1981

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..

CONTENTS

Page

Abstract .................................................................. . .. . 1

Introduction . .. ...................................... . ................. . .. .. . . 2

Purpose and scope ............................................... .. ....... .. 2

Methods .................................................................. . 2

location and description of study area ........ . .... . ......... ... .... ... .... . .. 2

Well-numbering system ................................................. ... . 2

Previous studies ........................................................ . . .. 4

Acknowledgments ...................................................... .... 4

Geology .................................................................. .. . 4

Stratigraphy ................................ .. .... .. .... . ..... . ......... . . .. 4

Gulfian Series (Upper Cretaceous) ......... . ..... . .. ... ......... . ...... ... . 4

Cusseta Sand equivalent ........................................... .... 4

Ripley Formation equivalent ....................................... .... 4

Providence Sand equivalent .... . ........... .. ............... .. ... ..... 4

Paleocene Series .............................. .. ............. .... ..... .. ,9

Clayton Formation .... . . . .. .. ..................................... ... .9

Nanafalia Formation and Tuscahoma Sand, undifferentiated .......... ... . 9

Eocene Series ................................ ... .................... . . . . 9

Hatchetigbee, Tallahatta, and lisbon Formations, undifferentiated .... . ... . 9

Ocala limestone ....................................... . .......... ... 11

Residuum ............................... . .... .......... . ... .. .... ... . .. 11

Hydrology .................. ... .......... . ................................. .. 11

Aquifer properties ............... ... ........ .. ...... . .... . ....... .. ... .. .. . 11

Providence aquifer ....... . .... , .... .. ........ .... ..................... .. 11

Clayton aquifer .. .... ......... . . . ..... . ............................... .. 13

Tallahatta aquifer .. . ................................ . .......... . ..... ... 13

Ocala aquifer ........................................................ .. . 13

Influence of the Flint River ........................................ ... 16

leakage ................................................................ ... 16

Multiaquifer hydrology .............................................. ... ... . .. . 16

Well construction ................ . ...................................... . .. 16

Flow through idle multi aquifer wells ............... . ........... . ......... .. . . 19

Areal trends in aquifer yields ............................................. . . . 20

Ground-water use ........... ..... .. ... .. .. .... .. . ..... .. .... .... .... ...... ... 21

Industrial ................................. ... .......................... . .. 21

Agricultural ............................................................ . . . 24

Municipal ........................................ . ..................... ... 24

Municipal pumpage from the Providence, Clayton , and Tallahatta aquifers . . . 24

Ground-water levels ....................................................... . .. 25

Potentiometric surface characteristics ......... . ..... . .......... . ........ . .. . . 25

Clayton aquifer . .. .. ...................... . ........ .... .. .. . . . .......... 25

Tallahatta aquifer ............... . ..................... . ........ . ..... . .. 25

Ocala aquifer ............ .... .... .... . . .. . . .. . . .... .. ................ ... 25

Long-term water-level declines ............... . ................. . ........ ... 25

Seasonal fluctuations in ground-water levels ..... . ......................... .. . 28

Conclusions and suggestions .............. .. ............... . .......... . ...... . . 28

Providence aquifer ........................... . .......................... ... 29

Clayton aquifer ....... .. .......................................... .. ..... .. 30

Tallahatta aquifer .................................. . .................... . . . 30

Ocala aquifer .................................... . ..................... . . .. 30

"

Suggestions ............................. . ............................. , 31

Selected referen<::es ..... .. .. ........ .. .... . .............. .. . ... . .. . ..... ... .. . 31

ii i

Plate

ILLUSTRATIONS
[Plate is in pocket]
1. Map showing well locations and the potentiometric surface of the Clayton and Tallah atta aquifers in the Albany Mea. GeorgiJ, September 1979.

Page

Figure

1. Map of G eorgia showing location of th e study area and physiographic districts of the

western Georgia Coastal Plain ...................... ... .. ........ .. ... ... ... . 3

2. Geologic section of the Albany area ........................................... . 6

3. Stratigraphic section and geophysical well logs at well95-08 at Albany ............ . 7

Figures

4-7 . Map showing:

4. Approximate altitude of the top of the Providence Sand ........... . ............. . 8

5. Approximate altitude of the top of the Clayton Formation ... .... . .. ......... .... . 10

6. Approximate altitude of the top of the Lisbon Formation .................. . ..... . 12'

7. Approximate transmissivity of the Clayton aquifer ........... . .. . .. .... ..... ..... . 15

Figure

8. Graph showing daily precipitation at Albany-Dougherty County airport, 1978 ...... . 17

9. Graph showing mean daily stage of th e Flint River at Albany, 1978 ................ . 17

10. Hydrograph showing daily water-level fluctuations in the Ocala aquifer at well95-03, 4

miles southeast of Albany, 1978" ........ .. .................... ... .. ... ...... . 18

11. Hydrograph showing daily water-level fluctuations in the Ocala aquifer at well95-22,

near the Worth-Dougherty County line, 1978 ................................ . 18

12. Sketch of typical multi,lquifer well construction ................................. . 19

13. Diagram showing direction and velocity of flow in city of Albany wells 95-33 and 95-34

when wells were not pumping ......................... .. .. .... .... .. . .... . . 20

14. Map showing results of flowmeter tests and the percentage of multiaquifer well yield

from the Clayton aquifer ... ... ... .. .... ....... .... ...... .......... ....... . . 22

15. Map showing results of flowmeter tests and the percentage of multiaquifer well yield

from the Tallahatta aquifer ................................................. . 23

16. Graph showing yearly ground-water withdrawal by Albany supply wells, 1969-78 ... . 24

17. Graph showing total daily ground-water withdrawal by Albany supply wells, 1978 .. . 25
18. Graph showing estimated monthly mean pumpage by the city of Albany from the

..

Providence, Clayton, and Tallahatta aquifers, 1978 ............................ . 26

19. Map showing potentiometric surface of the Ocala aquifer in the Albany area,

November 1979 ............... , .............................................. . 27

20. Graphs showing average daily pumpage from Albany supply wells, 1974-78, and aver-

age water-level fluctuations in the Clayton aquifer at well 95-09 near

Albany, 1970-78 ................................... .... ............ ... ..... . 28

21. Hydrograph showing daily water-level fluctuations in the Clayton aquifer at well95-06

at Albany, 1978 ........................................................... . 29

22. Hydrograph showing daily water-level fluctuations in th e Tallahatta aquifer at well

95-05 at Albany, 1978 ..................................................... . . 29

Table

TABLES
1. Generalized stratigraphy. water-bearing properties, and water-quality characteristics of formations underlying the Albany area . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5
2. Chemical analysis of well and river water, Albany area .. . . . ....................... 14 3. Estimated ground-water us e in the Albany area, 1978 ............................. 21

iv

FACTORS FOR CONVERTING INCH-POUND UNITS TO INTERNATIONAL SYSTEM (SI) UNITS

Multiply

By

To obtain

feet (ft) inches (in) miles (mi) square miles (m2) gallons per minute (gal / min) million gallons per day (Mgal/ d)

0.3048 2.540 1.609 2.590 0.06309 0.04381 43.81

meters (m) centimeters (em) kilometers (km) square kilometers (km 2) liters per second (Lis) cubic meters per second (m 3/s) liters per second (L/s)

feet squared per day (ft 2/ d)

Transmissivity 0.0929

meters squared per day (m1/ d)

National Geodetic Vertical Datum of 1929 (NGVD of

1929). A geodetic datum derived from a general

adjustment of the first-order level nets of both the



United States and Canada. It was formerly called "Sea

Level Datum of1929" or "mean sea level" in this series

of reports. Although the datum was derived from the

average sea level over a period of many years a~ 26 tide

stations along the Atlantic, Gulf of Mexico, and Pacific

Coasts, it does not necessarily represent local mean

sea level at any particular place.

v

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GEOHYDROLOGY OF THE ALBANY AREA, GEORGIA by
D. W. Hicks, R. E. Krause, and J. S. Clarke

ABSTRACT

From 1960 to the present (1978), the Albany-Dougherty

limestone comprising the aquifer becomes thinner and less

County Metropolitan Area of southwest Georgia has expe-

permeable.

rienced a period of rJpid growth. This rapid growth has

Due to the relatively low hydraulic conductivity of the

caused ground-water use to more than triple during the past 20 years, presently Jver<~ging <lbout 39.4million gallons

Providence, Clayton, and Tallahatta aquifers, large groundwater withdrawals in the Albany area have produced

p(r day. L;:nge withdrawals in the Albany area have caused water levels to declinl~ in one aquifer as much as 135 feet

widespread depressions in the potentiometric surface of each aquifer. Accelerated agricultural use of the Clayton

since 1940.

aquifer to the northwest in parts of Dougherty, Terrell, and

Ground wJter in the Albany area is obtained from four

Calhoun Counties has elongated and expanded the cone of

aquifers of Late CretJceous to middle Tertiary age that

depression at Albany about 14 miles in that direction.

range in depth from about 40 to 960 feet below land surface.

Increased pumpage could limit the availability of water

From deepest to shallowest the aquifers ilre: the Providence

from the Clayton aquifer.

(sand), the Clayton (limestone), the TJIIahatta (sand), and

Heavy pumping has increased the naturally occurring

the Ocala (limestone). Ground water is present in the

head differences between the Providence, Clayton, Talla-

underlying Cusseta S<1nd at depths of about 1.250 to 1,500

hatta, and Ocala aquifers in the Albany area and has

feet; however, high drilling costs, low yields, and excessive

enhanced the possibility of leakage of Wdter through the

concentrations of chloride (422 milligrams per liter) and

intervening confining layers that separate these aquifers.

dissolved solids (1 ,610 milligrams per liter) in Cusseta waters

The tot<ll amount of leakage from the Providence into the

make development of this unit undesirable.

Cl.1yton and from the Ocala into the Tallahatta, and the

..

Well yields range from less than25 gallons per minute in the Providence and Clayton aquifers, to more than 2.000

Meal extent of this leakage, is presently unknown. Brinetrace studies made in eight wells at Albany indicate that in

g<~llons per minute in the Ocala aquifer. Areal variations in

addition to leakage through confining layers, about 1.1

the hydraulic conductivity of the Providence, Clayton, and Oc.li<~ aquifers cause yields to vary throughout the Albany

million gallons of water per day rechJrge the Clayton aquifer through idle multiaquifer wells that also penetrate

area. The productivity of the Providence and CIJyton

the Providence and Tallahatta aquifers of higher head.

aquifers progressively increases toward the west and north-

Water in the Providence, Clayton, Tallahatta, and Ocala

west parts of the area, where well yields of about 2,000

<~quifers is suitable for most uses and generally contains no

gallons per minute are reported from the Clayton. The

constituent concentrations that exceed the Georgia Envi-

Tallah;'ttta aquifer generally yields from 1,000 to 1,400

ronmental Protection Division and U.S. Environmental

g<~llons per minute to wells and docs not exhibit significant

Protection Agency standards for safe drinking water.

areal variations in hydraulic conductivity throughout the

However, in areas where the Ocala is poorly confined or is

report area. The productivity of the Ocala aquifer decreases

in direl t contact with surface w,1ter.localized water-quality

in the west dnd northwest parts of the area where the

changes .ne possible.

INTRODUCTION

aquifers used for water supply in the i\rea or the

From 1960 to the present (1978), the AlbanyDougherty County Metropolitan Area in southwest Georgia has experienced a period of rapid growth. This rapid growth has caused ground-water use to more th an triple during the past 20 years. Long-term large ground-water withdrawals have caused the water level in one <:~qui fer to d ecl ine as much as 135ft since 1940.
The use of ground water for irrigation is rapidly increasing to the west and northwest of Albany in parts of Dougherty, Terrell, and Calhoun Counties. The increased agricultural use in these areas could affect ground-water avail<lbility in Albany.
Most municipal wells in the Albany area tap two or more of the four ground-water reservoirs present. Because of multiaquifer well construction, almost nothing was known about the water-bearing or water-quality characteristics of individual aquifers

underlying water-beari11g u11it. Geophysical logs w er e made in these and other wells throughout th e study area to gain a better und erstanding of the ~tratig raphy, the nJture of th e hydrologic sys tem, c1nd the water quality. Continuous drill co res we1e collect ed in test well95-01 from land surface toil depth of about
1,400 ft. Flowmeter surveys were m<ide in six multi-
aquifer city wells to estimate th e reiJtive yields from specific water-bearing zo n es. Borehol e-flow ,malyses were made in eight multiaquif er production w ells where the dir ect ion Jnd velocity of flow in the well bores were re co rded in order to estimate the relative head in each aquifer under pumping stress. Continuous water-level recorders were installed on 11 test wells to monitor water-level flu ctuations. Water-use and water-quality data were coll ected to gain a better understanding of the long-term effects of heavy pumpage on the ground-water system.

prior to this investigation. Although waters from the four aquifers tapped in

Location and Description of the Study Area

the Albany area generally are of good quality, the

The study includes parts of Lee, Terrell, and

deeper water-bearing zones underlying these aqui- Mitchell Counties and most of Dough erty County,

fers yield water having concentrations of chloride and

e ncompassing a total area of approximat e ly 390 mi 2

dissolved solids that exceed the safe drinking water

(fig. 1).

standards. Head differentials resulting from declining

With the exception of the extreme southeast and

water levels in the heavily used aquifers may acceler-

northwest corners, the entire study Jrea lies within

. ate the infiltration of poor-quality water from the

the Dougherty Plain district (fig.1) of the CoastJI Plain

underlying zones.

province of Georgia (LaForge and other s, 1925). The

To better manage th'e water resources in the Dougherty Plain is bordered on the east by the Tifton

Albany area, municipal, industrial, agricultural, and

Upland and on the west by th e Fall Line Hills. The

'

other water users need to know the deve lopment study area is che1racterized by a relatively lev el or

potential of the vital ground-water resource. Recog- gently undulating topography, where altitudes range

nizing this, in 1976 the city of Albany and the Georgia from 160 to 280ft. Conspicuous round to irregularly

Department of Natural Resources, in cooperation

shaped depressions mark the southwest and north-

with the U.S. Geological Survey, began an investiga- east parts of the study area. Th ese depressions are

tion to evaluate the ground-water resources of the sinkholes caused by solution of limestone bedrock

Albany area.

followed by subsurface collapse, and are typical

Purpose and Scope

surface features in karst terrane. The Flint River and its tributaries, including Kin-

The purpose of this study was to evaluate the development potential of the ground-water resour-

chafoonee, Muckalec, Kiokee, Coolecwahee, and Piney Woods Creeks, drain the study area.

ces in the Albany area. To properly analyze the ground-water system the following hydrologic fac-

Well-Numbering System

tors were evaluated: the head and water quality in

This report utilizes a well-locating system in which

each aquifer utilized; the head and water quality of the wells are numbered serially in each county. Each

the underlying water-bearing zo nes; and the relative well is assigned a county number and a sequen ce

yields supplied by the Providence, Clayton, and

number within that county. Accordingly, well number

Tallahatta aquifers to multiaquifer production wells.

95-01 represents well number 1 locat ed in county 95.

Methods

From this number the exact location of each well ca n be obtained from the index of ground-water sites on

Since this investigation began in 1976, the U.S. Geological Survey has drilled a total of 12 test wells in the Albany area (pl. 1), each tapping one of the four

plate 1. Counties and their respective numbers used in the well-numbering system ar e: Calhoun, 37; Dougherty, 95; Lee, 177; and Terrell, 273.

2

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10

20

30

40

50 MILES

Figure 1. Location of the study area and physiographic districts of the western Georgia Coastal Plain.

Previous Studies
Little detailed hydrologic investigation has been done in the Albany area. Stephenson and Veatch (1915) discussed the geology, hydrology, and water quality in a general context. Herrick (1961) presented paleontologic and lithologic descriptions of three wells in the Albany area. The most complete study in the Albany area was done by Wait (1963), with the resulting report containing data collected through 1957. However, the hydrologic data in Wait's report were obtained primarily from multiaquifer wells.
AcknowledGments
This investigation was conducted by the U.S. Geological Survey in cooperation with the Georgia Department of Natural Resources, ~nvironmental Protection Division, Georgia Geologic Survey, and the city of Albany Water, Gas, and Light Commission.
The Layne-Atlantic Co. (Albany) staff was extremely helpful in furnishing historical records, and provided many opportunities to conduct borehole investigations in the area. Special thanks are due Miller Brewing Co., Georgia Power Co., and St. Joe Paper Co. for allowing the U.S. Geological Survey to drill test wells on their properties, and to Miller Brewing Co. for the opportunity to particjpate in aquifer tests on their property in Albany.
The writers wish to extend special thanks to Mr. Walter Rodemann, General Manager of the Albany Water, Gas, and Light Commission, for his assistance, and to the many cordial people of the Albany area who provided useful historic information and allowed the use of their wells for water-level measurements.
GEOLOGY
The Coastal Plain sediments underlying the study area consist of alternating units of sand, clay, shale, and limestone (table 1 and fig. 2). The sediments extend to a depth of at least 5,000 ft and dip to the southeast by as much as 25 ft/mi, progressively thickening in that direction.
The sedimentary units show lateral variations in lithology and thickness that represent changing environments throughout the depositional history of the area. Transgressions and regressions of the sea caused the depositional environment at any given locality to change from one depositional cycle to the next. Where changes in sea level were rapid, a transitional sequence may be missing from the sedimentary record.
The original thicknesses of the individual lithologic units were controlled by the length of deposition and the sedimentation rate. Moreover, since

deposition, the units have been modified in thickness and composition by weathering, erosion, compaction, and chemical alteration.
Stratigraphy
Gulfian Series (Upper Cretaceous)
The Upper Cretaceous Series in the outcrop area can be divided into six formations (Cooke, 1943). From oldest to youngest they are: the Tuscaloosa, Eutaw, and Blufftown Formations, the Cusseta Sand, the Ripley Formation, and the Providence Sand (table 1). The Cusseta Sand, Ripley Formation, and Providence Sand were the only Upper Cretaceous formations investigated during this study. Due to similar lithologies, these formational contacts in the Albany area are not definite and figure 2 represents only the approximate stratigraphy of this series. Figure 3 shows the Cusseta, Ripley, and Providence stratigraphic sequence partially penetrated by test well 95-08 in Albany, along with selected geophysical logs that reflect the different lithologies. The Cusseta, Ripley, and Providence sequence was penetrated fully at oiltest well 95-12 in western Dougherty County, where the thickness of the sequence is about 640ft.
Cusseta Sand equivalent In the report area the Cusseta Sand is a silty,
micaceous, calcareous sand containing thin layers of interbedded shale. Glauconite is abundant in the deeper zones, but becomes less prominent higher in the section.
Ripley Formation equivalent Overlying the Cusseta Sand is a sedimentary unit
that corresponds stratigraphically to the Ripley Formation. The absence of definite lithologic breaks makes establishing formational contacts difficult, if not impossible. The lower part of the Ripley consists of fossiliferous claystone containing interbedded sand partings and fine sand. The claystone grades upward into a massive siltstone that is slightly calcareous and clay rich. In the upper part of the formation the clay is completely absent, and the Ripley consists of tight, fine to medium, micaceous sand.
Providence Sand equivalent The Ripley Formation is overlain unconformably
by the Providence Sand. The basal unit of the Providence consists of a slightly dolomitic coquina that grades upward into a fossiliferous siltstone. The upper part of the Providence is a very fine- to coarse-grained calcareous, clayey, micaceous sandstone.
Figure 4 was constructed using geophysical logs from 10 wells in the Albany area and shows the approximate altitude of the top of the Providence

4

Table 1.

Generalized stratigraphy, water-bearing properties, and water-quality characteristics of formations underlying the Albany area.

r=T Era

Series

I I Quaternary

Pleistocene

Oligocene

Gulf Coast Stage
j Vicksburgian
Jacksonian

Group and
Formation
Dune sand
Terrace deposits Flint River Formation
Ocala Limestone

1Thickness
(feet) I

Lithology

0-35

I Fine to coarse, well sorted, angular to subangular quartz sand

I

I 0-20 Poorly sort:ed gravel, sand, and clay

Water-bearing properties Not water bearing Not water bearing

Water-quality characteristics

Light-gray, cherty limestone

Properties unknown

White to light-pink, fossiliferous limestone

Ocala aquifer is a very productive water-bearing unit: throughout the Dougherty Plain. Reported well yields of more than 2, 000 gal/min. Yields decrease north and west of Albany

I Slightly glauconitic, fine, calcareous Limited water-bearing potential--used only in mul-
sand, clay, and interbedded limestones tiaquifer wells where other aquifers are tapped

Quality unknown
Water is generally a hard calcium bicarbonate type that meets all State drinking water standards (1977)

Lower Paleocene

I

0.

" 0

Midwayan

"" '

!"'

"'

I Navarroan

Clayton Formation (upper unit)
Clayton Formation (limestone unit)
Clayton Formation (lower unit)
-
Providence Sand
Ripley Formation

40-120

Fine to medium sand, clayey sand, and interbedded limestone layers that are very fossiliferous at the top of the formation

Tallahatta aqul.l.er is a major aquifer in the Albany area; used for municipal, agricultural, and industrial supplies. Reported well yields of as much as 1,400 gal/min

Very tine, green-sraine<Iqua----rt-z samf", locally calcareous and glauconitic

Aquifer is tapped by many multiaquifer wells; however, water-bearing properties unknown

I Fine to medium, micaceous, clay-rich

Used in. some multiaquifer wells; water-bear1ng

sand. Glauconite is abundant through- propert1es unknown

out. Lower part is nonfossiliferous,

clay-rich sand (pccasionally greater

than SO percent clay)

I Fine to medium, calcareous quartz sand Used in some multiaquifer wells; water-bearing

and interbedded thin limestones

properties unknown

Water is a hard calcium bicarbonate type that meets all State drinking water standards (1977) and is sui table for mast uses
Quality unknown

70-125 15-40

Massive, light-gray, recrystallized limestone. Very fossiliferous at the top of the unit
Fine to medium, arkosic sand, locally glauconitic and silty

Clayton aquifer is a major aquifer in the Albany area. East of Albany the aquifer is a poor producer; however, to the west and northwest, well yields as great as 2,000 gal/min have been re_eorted
Water-bearing properties unknown

The Clayton aquifer produces water that is suitable for municipal, agricultural, and industrial supply. It is generally a soft sodium bicarbonate type that meets all State drinking water standards (1977)

)2,500

Upper part of unit is a dense, gray, clayey sand. Middle part is generally a coquina. Lower part is sand containing varying amounts of silt

Providence aquifer is used in the Albany area for municipal and industrial supply. Yields range from less than 25 to about 500 gal/min

Fine to medium, calcareous sand and fossiliferous claystone

Not water bearing

Water from this aquifer is a soft sodium bicarbonate type that is suitable for most uses and meets State drinking water sta~dards (1977)

Cretaceous
!:!
0
I;"";
"'

Gulf ian

Comanchean

Tayloran
Austinian
II Eaglefordian Woodbinian
----
Washi tan, Fredericksburgian, and
Trinitian

Cusseta Sand
Bluff town Formation Eutaw Formation
Tuscaloosa Formation
Undifferentiated

Fine, micaceous, calcareous sand containing varying amounts of silt and clay

Not used as an aquifer in the Albany area; however, in other areas of Georgia yields as great as 500 gal/min have been reported

Water is a soft sodium bicarbonate type that has concentrations of chloride and dissolved solids that exceed State drinking water standards (1977)

Alternating layers of sand, sandy clay, and clay

Not used in the Albany area

Water quality is about the same as that in the Cusseta and does not significantly change through the Tuscaloosa. Below the Tuscaloosa, the concentration of sodium chloride is reported to increase significantly

A

A'

-44

232 It

95-08

~---:.;-~~.:.~,:9;~-~,.~f;..t- - - - - -- -- ----;:;Res, uuu ...

Ocala Limestone

lisbon, Ta/lahatta, Hatchetigbee
Formations, undifferentiated

Tuscahoma Sand and Nanafa li a Fo r mation, undif feren ti a t ed

Ol

Uppe, unit of ClaYton Fo,motlon

limestone Unit of Clayton Fo,motion

9001 1000'
lloo' 1200'

EXPLANATION
t:""-3) Sandy cloy
~ Limestone
W'(i'J Send WI+tj Coquina
m Silty limestone
lf+.jj Calcareous sand

Providence Sand

- -- - --t-=_-::-<><__,_

Ripley Formation

_?_ _ - ?

?

Cusseta Sand- -- - -- - r-~

? I I

)!II [fI

f MILES

Vertical exaggeration X 35 Notional Geodelic Verftcol Datum of 1929

Figure 2. Geologic section of the Albany area .

\.

SPONTANEOUS

NATURAL

POTENT I A L RESISTIVITY

GAMMA

0

100' 200'

Ocala aquifer

300' 400'

Tallahatta aquifer

500' -

Confining unit

600 ' -

700'
eoo' -
900' -
Total depth 1360 feet

Clayton aqu i fer
Confining unit
Providence aquifer
Confining unit
EXPLANATI ON
~. Sandy cloy ~ Limestone ~< Sand ~ Coquina ~. Calcareous sand
D Cloy
Vertical exaggeration X35

75 50 25 0 100 200 300 MILLIVOLTS OHM-METERS

0

100

200

COUNTS PER SECOND

Figure 3. Stratigraphic section and geophysical well logs for well 95-08 at Albany ..

7

84 15'

8400'

to

3130'

/ /

-585
Bose from U. S. Geological I: 24,000 quadrangles

0() /'()
~

I
0/
~0
/

0

5

EXPLANATION

-723

STRUCTURE CONTOURShows approximate altitude of top of Providence Sand. Contour interval 100 feet. Notional geodetic vertical datum of 1929
of top of Providence Sand

DOUGHERTY
MiTCHEu::-- -

10 MILES

Figure 4. Approximate altitude of the top of the Providence Sand.

Sand. Depths to the Providence can be estimated throughout the study area by reading from figure 4 the approximate altitude of the formation and subtracting this from the land-surface altitude.
Geophysical well logs indicate that the Providence thickens downdip to the southeast. From figure 4, an average dip of about 23 ft/mi was computed for the top of the Providence Sand.
Paleocene Series
The Paleocene Series consists of the Midway Group and part of the Wilcox Group (table 1). The Clayton Formation is the only unit of the MidwJy Group recognized beneath the study area, and it unconformably overlies the Upper Cretaceous Providence Sand. The Nanafalia Formation and Tuscahoma Sand undifferentiated represent the lower part of the Wilcox Group in the study area, and unconformably overlie the Clayton.
Clayton Formation The Clayton FormJtion in the study area can be
divided into three lithologic units. The lowermost unit is a fine to medium calcareous sand containing varying amounts of silt and glauconite. The middle unit is a massive limestone composed of highly calcitized fossils in a recrystallized, slightly sandy limestone matrix that forms a tough, coherent rock. The sand content of the limestone increases upward, with the rock becoming less coherent. The upper unit consists of fine to medium, calcareous, quartz sand containing minor glauconite and varying amounts of silt and clay.
Variations in lithology also occur laterally in the Clayton Formation. Downdip, to the southeast, the clay and silt content in the limestone increases sharply, filling the pore spaces and causing a decrease in effective porosity and permeability.
Due to irregularities developed on the surface of the underlying formations prior to deposition of the Clayton, to extensive post-Clayton erosion, and to solution of the middle limestone unit, the surface configuration and thickness of the Clayton Formation vary throughout the study area. The average thickness of the entire formation ranges from about 180ft in the northwest part of the area to about 245 ft in the southeast part. The limestone part of the formation ranges in thickness from about 125ft in the northwest to about 70ft in the southeast. Figure 5 shows that the Clayton Formation generally dips to the southeast at a rate of about 17ft/mi. The dip rate increases in the southeast part of the area to about 22ft/mi.
Nanafalia Formation and Tuscahoma Sand, undifferentiated
The Clayton Formation is unconformably overlain by the Nanafalia Formation and the Tuscahoma Sand,

undifferentiated. The basal part of this sequence grades upward from a nonfossiliferous sand and clay to a fine to medium, calcareous, fossiliferous sand. The upper part consists of a fine, slightly micaceous, clay-rich sand. Glauconite is abundant throughout, composing approximately 50 percent of the sediment in some clay-rich zones.
The thickness of the Nanafalia-Tuscahoma sequence is fairly uniform in the study area, increasing only slightly downdip to the southeast where it attains a maximum thickness of about 120ft (fig. 2).
Eocene Series
Eocene sediments of the Hatchetigbee, Tallahatta, and Lisbon sequence represent the entire Claiborne Group and the upper part of the Wilcox Group in the study area, and unconformably overlie the Paleocene Tuscahoma Sand. The sequence is difficult to subdivide in the report area because it consists throughout of lithologically similar alternating layers of thin- to medium-bedded sands, sandy clay,s, and siltstones, all of which are highly glauconitic and commonly calcareous (fig. 2). Minor beds of white- to medium-gray limestone are present. Coarse, broken oyster shells are prominent in the limestones and calcareous sands and are the only macrofauna that occur in the sequence.
Hatchetigbee, Tallahatta, and Lisbon Formations, undifferentiated
In the absence of any definite lithologic or faunal breaks, the following informal subdivision of the Hatchetigbee-Tallahatta-Lisbon sequence is used in this report. The predominantly clayey section immeuiately overlying the Tuscahoma Sand is thought to be the Hatchetigbee Formation in the study area. Overlying the predominantly clayey Hatchetigbee Formation is a section that consists primarily of fine to medium sands and clayey sands. Thin limestone beds are interlayered throughout the middle and upper parts of the section. In the study area the limestone beds are more fossiliferous near the top of the section where they are replaced by a thick layer of coquina. The sand, limestone, and coquina section is the part of the Eocene most commonly used as an aquifer and is herein referred to as the Tallahatta Formation. The uppermost part of the sequence is predominantly clay, much like the Hatchetigbee, and contains prominent beds of calcareous, glauconitic sand and limestone. This section is herein correlated with the Lisbon Formation.
The Hatchetigbee, Tallahatta, and Lisbon Formations, as subdivided here, are considered to be "operational" stratigraphic units whose gross lithologic characteristics can be correlated for reasonable distances and which generally fit a currently accepted stratigraphic division.

9

TERRELL DOUGH ERTYb
/~oO
/ - 3 1 5

0

3130'

/e410

Base from U.S. Geological Survey

0

I: 24,000 quadrangles

00
/~
/ /
/ /

~
~(J
// -545
EXPLANATION r-.:xJu- STRUCTURE CONTOUR-
l Shows approximate altitude
of top of Clayton Formoti on.
I Contour interval 100 feet. I
Notional geodetic vertical datum of 1929
-545 DATA POl NT- Number is altitude, of top of Cl oyton Formation
DOUGH~R2!_ - -----l Mil'"""CH ELL
10 MILES

Figure 5. Approximate altitude of the top of the Clayton Formation.

<

The top of the Hatchetigbee-Tallahatta-Lisbon sequence dips to the southeast at approximately 10 ft / mi (fig. 6) and undergoes a marked increase in thickness downdip (fig. 2). The thickness of this sequence ranges from about 235ft in the northwest part of the area to about 340ft in the southeast.
Ocala Limestone The Ocala Limestone comprises the upper Eocene
Jackson Group in the report area and unconformably overlies the Lisbon Formation. The Ocala Limestone crops out in the study area along the Flint River and Kinchafoone e, Muckalee, and Piney Woods Creeks where erosion has removed the overburden .
The basal section of the Ocala consists of a tough fine- to medium-grained recrystallized, dolomitic, moderately fossiliferous limestone. The limestone is more sandy in the middle of the section where fossils are less abundant. Limestone near the top of the section is variably fine to coarse grained, chalky, and coarsely fossiliferous (P. F. Huddlestun, oral commun., 1980).
The Ocala dips slightly to the southeast at 2 to 5 ft / mi and generally thickens in that direction. The formation ranges in thick ness from about 150 to 200ft throughout the report area .
Residuum
Most of the Dougherty Plain part of the report
area is covered by 40 to 70 ft of unconsolidated
residuum developed from weathering of the Ocala Limestone and Oligocene limeston es. This residuum is generally a red sandy clay that, in the southeast part of the ar ea, may contain siliceous boulders as large as 3ft in diamet e r. The flood plain of the Flint River is covered by 20 to 70ft of unconsolidated river-terrace deposits.
HYDROLOGY
Water in the Albany area is obtained primarily from four ground-water reservoirs, or aquifers (table 1). From deepest to shollowest, the aquifers are: the Providence, Clayton, Tallahatta, and Ocala. Although ground water is pres e nt in the underlying Cusseta Sand, high drilling costs, low yields, and excessive concentrations of chloride and dissolved solids make development of this unit undesirable.
Recharge waters enter the aquifers where they occur near land surface and percolate downgradient to become confined between relatively impermeable beds of clay, sandy clay, or shale. Thus, confined ground water is under a constant pressure known as hydrostatic, or artesian, pressure. When a well penetrates a confined aquifer downdip from the recharge

area, artesian pressure causes the water in the aquifer to rise above the top of the aquifer. An imaginary surface connecting points to which water would rise in tightly cased wells is called the potentiometric surface (Lohman, 1972, p. 8). The altitude of the potentiometric surface is controlled by the artesian pressure and is a function of the rate of recharge, the hydraulic gradient (slope of the imaginary water surface), and the rate of discharge.
The transmissivity of an aquifer is defined as the rate at which water will flow through a unit width of material under a unit hydraulic gradient. It is, thus, a measure of the aquifer's ability to transmit water. Transmissivities used in this report are estimated from specific capacity data and, because of well losses, are generally lower than values calculated from aquifer tests. n.e hydraulic conductivity is also a term used to define the water-transmitting ability of an aquifer. Like the transmissivity, it is influenced primarily by permeability and hydraulic gradient, but is also influenced by the viscosity of the water.
The ability of many carbonate aquifers to transmit water is enhanced by the development of secondary permeability. Circulating ground water containing carbon dioxide dissolves calcium carbonate along joints and bedding planes in the aquifer, thus enlarging the primary flow channels as well as creating new channels.
Aguifer Properties
Providence Aquifer
The Providence aquifer receives recharge where it occurs near land surface along a northeast-trending line about 50 mi north-northwest of Albany . Ground water is confined in the aquifer from below by the dense clay of the Ripley Formation, and from above by th e silty upper Providence-lower Clayton sequence (fig. 2). Ground water is obtained from the Providen ce aquifer in the Albany area at depths ranging from about 640 to 960ft below land surface.
Artesian pressure in the Providence was sufficient during 1978 to produce an averag e water level of about 110 ft below land surface at well 95-08 at Albany, near the center of municipal pumpage. Water levels become higher with in creased distance from the pumping center.
Estimates of transmissivity for the Providence aquifer range from about 250 ft 1/ d at well 95-01, 3 mi southeast of Albany, to 1,000 ft 2/d at well 95-48, approximately 12 mi updip to the northwest. The hydraulic conductivity is lowest in the upper part of the formation and highest in the coquina bed (fig. 2) where most of the wate r is produced . The Providence

11

TERRELL

_.
1'.)
3130'
12
Bose from U. S. Geological I: 24,000 quadrangles

-67

EXPLANATION

- 0 - STRUCTURE CONTOUR-

Shows approximate altitude

of top of Lisbon Formation .

Contour interval 100 feet.

National geodetic vert i cal

-14

datum of 1929.

DATA POINT-Number is a

of top of Lisbon

DOUGHERTY
MiTCHEu---

0

5

10 MILES

Figure 6. Approximate altitude of the top of the Lisbon Formation.

yields less than 25 gJI/min to wells in the south and southeast parts of the report area where the transmissivity is low; however, updip to the northwest, yields to wells of .1bout 500 gal/min have been reported.
The Providence aquifer produces a soft sodium bicarbonate type wdter that contains no constituent concentrations that exceed the Georgia Elwironmental Protection Division st,Jndards (1977) for safe drinking water (table 2). The ,1verage calcium, magnesium hardness of 6 mg/L (milligrams per liter) and low average dissolved iron concentration of 50 ug/L (microgrJms per liter) 111<1ke water from this aquifer ideal for domestic use.
Clayton Aquifer
The Clayton Jquifer is recharged primJrily where it occurs near land surfJce and where the formation is exposed in steep valley wJIIs Jlong a northeasttrending line about 35 to 40 mi north-northwest of Albany. The topogrJphy of the Clayton recharge area is not co11ducive to the influx of large quantities of Wdter. Ground water is obt<1inable from the Clayton aquifer in the Albany area at depths ranging from about 550 to 840ft below land surface. The Clayton is artesiJn in the Albany Mea Jnd water in the aquifer is confined from below by the silty upper Providencelower Clayton sequence and from above by the clayey Tuscahorna Sand.
During 1978 the Clayton aquifer had an average water level of 140ft below land surface at well 95-06 (pl. 1) near the center of pumpJge in Albany. This was the lowest water level recorded in the Albany area.
Figure 7 shows how the transmissivity of the CIJyton aquifer varies later.JIIy, increasing from the area east of Albany, northwest to Sasser. Estimates of transmissivity, made from specific-capacity data (Lohman, 1972, p. 52), range from about 200 ft 1/d at well95-07, approximately 3 mi southl'JSt of Albany, to about 11,000 ft 2/d at well 273-03, to the 11orthwest at Sasser. Yields to wells tapping the Clayton aquifer, like those of the Providence, vary areally. Well95-09, approximately 3 mi northeast of Albany, produces about 250 gJI/min, whereas well 273-05 near Sasser has a reported production of about 2,000 gal/min. This progressive increase in transmissivity and yield toward the northwest is due largely to a directional increase in hydraulic conductivity and the thickening of the water-bearing part of the Clayton Formation.
Water from the Clayton aquifer generally is a soft sodium bicarbonate type that contains no constituent concentrations that exceed the State standards (1977) for drinking water (table 2). Although the average dissolved iron concentration of 152 ug/L is higher

than that in the Providence aquifer, the level is not excessive and hJs not been reported to cause staining or encrustation problems.
The sodium bicarbonate water in the Clayton Jquifer is nontypical of carbo11ate aquifers, which generally yield water of a calcium bicarbonate type. The uncharacteristically high concentration of sodium (average 44 mg/L) in water from the Clayton in Albany could result from the leakage of sodium bicarbonate w<Jter from the underlying Providence aquifer.
Tallahatta Aquifer
The Tallahatta aquifer is recharged primarily by rainfall where the sediments occur near land surface along a northeast-trending line 20 to 30 mi northnorthwest of Albany. The Tallahatta aquifer is comprised of several hydraulically interconnected waterbearing zones in the Hatchetigbee-Tallahatta-Lisbon sequence. Ground water can be obtained from this aquifer in the Albany area at depths ranging from about 125 to 350ft below land surface. The aquifer is confined from below by the clayey Tuscahoma Sand and from above by the upper part of the Lisbon Formation. During 1978, artesian pressure in the Tallahatta aquifer was sufficient to produce an average water level at well95-05, near the center of pumpage in Albany, of about 90ft below land surface.
Limited areal testing indicates that the transmissivity and yield of the Tallahatta aquifer does not vary significantly in the Albany area. Estimates of transmissivity, made from specific-capacity data, range from about 2,400 to 3,500 ft 2/d. The water-bearing potential of the Tallahatta aquifer is good where tested and yields to wells of 1,000 to 1,400 gal/min have been reported. However, the relatively low transmissivity of the aquifer results in large drawdowns when pumpage exceeds about 750 gal/min.
The Tallahatta aquifer produces a hard calcium bicarbonate type water that contains no constituent concentrations th<lt exceed the State 1977 drinking water standards (table 2). The dissolved calcium concentration ranges from 18 to 52 mg/L and is uncharacteristically high for a predominantly sand aquifer. Although dissolution of calcite could account for part of the dissolved calcium, the relatively high calcium levels observed in water samples from the Tallahatta aquifer in the Albany area could result from the vertical leakage of calcium bicarbonate water from the overlying Ocala aquifer.
Ocala Aquifer
The Ocala Jquifer is recharged,~n the Albany area and throughout much of the Dougherty Plain, chiefly

13

Table 2.

Chemical analysis of well and river water, Albany area. (Analyses by U.S. Geological Survey. <,less than)

Site number

Owner or name

Aquifer

Dote

sampled

I ..
EN

.
u

-;o 3

.~~ -~ ;,

u

~

Milligrams per liter

~

.
z
~
j

3
j
.0

..u0
~ "'
6
]..

Q
""0 0~
~u
......-<
~u
<.

..ei5
.-< 0
"'

Dissolved Ha r dn..,

solids

M1.crograms per liter

....
u
~
" ~'"
u

.;;:
~
."""0"
0 .-<

. -
~
. . 0
3
""""

6z '
~
u
..00
.""' ~.-.
z "o'u.

~!-'

.. .. H ...... ;~ . "0
. ... .. ... ~0""u
E c
.. ~ 3

,- "0" ~'"0"
~

u .-<

"

0u"

u. "

u 0
~ ~'"u
~~
~ 6
""'"~"

3 '

~"-~ 3 .,
"'" ~""

:a " ,.., ~ ~"""~ ~-;j

o~ ,0 N

.-<.Q
83

5~

...
<
~
3
..'i
0
;;l

~
u
"~"
<

. ." ~ .,
u

u
~

~
0

~

u

, 3 ~

~ ~
e o
"u .u'c"

'" u ""0 " "

.
~ "'
c
0
" ~

~

. ~
...,

~
:~ ;


~ ""'' "u,"'

. . . ...

c
"

"'"

."'
E

"'0"'

~ ~"" 0
~ c
"'

f
u
" ~
N

Drinking water standards 1./

95-12 Se:.aly, .) , R., l

95-12

Do .

95-DI uses tw j . Albany

95-08 USGS n> 10, Albany

Cusseta do. do.
Providence

10-15-57 15 06-27-78 II 06-17-77 13 11-21-78 12

5.2 2.3 586 6.9 2.2 620 4.3 .8 660 1.7 .4 85

5.6 820 689 5.7 850 700
.2 1,040 850 1.6 200 190

0

0

~

~

N

N

0

0

0

0

~

~

0.0 435 2.6

-

- 1,500 1,470

7.6 420 4.3 410

4.0 0.09 o.oo 1,510 I ,500

- 3.2

-

- 1,610

7.6 2.4 .6 .09 .oo 214 223

~

8 ~ g ~...;-

- - - 22 0 2,490 8.4 22.0 22 5.2

--

27 0 2,100 7.5 25.0 20 43 30 2 0 0 0

14 0 2,575 8.2 21.0 60 10 10 I 0 0 0

6 0 358 9.2 24.0 0 .2 40 0 3 I 0

0 0
~

c

0
~

~

N

g

- - - --

8
"'
--

20 3 30 <0.5 0 430 10

10 0 0 50 10 0

0 0 360 0
.6 0 - 0

95-06 U9..GS n.'l 6 1 .Ubany 95-07 trSGS l\1 1, ..Ub.my

Clayton do.

03-07-78 20 12

6.0 33 2.8 140 110 13

1.5 .2 .04 .00 160 158 55 0 231 7.2 22.8 10 14 20 0 0 0 0 180 11 10 <.5 0 360 0

05-31-78 25

8.6 2.4 80 3.1 230 190 4.2 4.5 7 .00 .00 241 243 32 0 284 8.0 21.7 10

- 40 2 0 0 7 110 0 10 <.5 0 380 0

177-02 uses T\J 9' Albany
95-09 nune.r crcy , CJ ., 2

do.

09-28-78 19 IS

6.0 30 2.9 140 110 14

1.9 .2 .00 .00 157 159 63 0 252 7.7 21.9 5 45

0 0 I 0 0 120 13 10 <.5 0 410 0

do.

08-16-55 21 11

5. 7 40 2.8

- - 12

2.5 .2 .40

- - - - - - - 162 169 50 0 256 7.6 22.7 8

-

-

80 - -

--

95-09

Do,

95-09

Do .

_.

95-02 USGS 1:W 2 , IJ.~ony

~

95-D4 USGS 'IW 4 1 Al.b.II\Y

do. do. Tallahatta do.

04-28-76 18 II

5.1 39 3.3 146 120 12

2.7 .3 .oo .03 170 164 49 0 263 6. 7 24.0 0 47

0 0 0 0 0 170 0 0 .I 0 270 0

06-21-78 18 10

4.9 34 2.8 140 110 9.4 1.7 .2 .09 .oo 163 156 45 0 259 6.6 24.0 5

- - 20 1

0 0 250 8 10 <.5 0 260 10

06-17-77 40 30 10

13 4.3 177 ISO 6.3 4.5 .1

-

- 188 196 120 0 288 7.6 22.5 5

- 10 I 0 0 0

60 0 10

0 0 420 0

I0-2Q-77 32 50

2.6 4.0 1.4 170 140 5.1 2.5 .I .04 .oo 190 182 140 0 276 7 .I 21.0 2 22

0 I 0 I 0 190 3 0 (.5 0 410 10

95-D5 USGS n.~ 5, Albany

do.

02-D9-78 33 52

8.3 9.0 3.2 210 170 6.0 4.1 .1 .00 .00 212 220 160 0 350 7.6 21.0 10 8.4 40 4 0 0 I 230 0 0 <.5 0 320 10

177-0 1 USGS 1'ol S, Al.b..ny

do.

09-25-78 34 37

6.9 16 2.5 170 140 10

3.0 .2 .oo .DO 187 194 120 0 289 7.6 22.0 0 6.8 0 0 0 0 0

70 I 10 ( .5 0 420 0

95-10 USGS 1'11 l!, Allw.ny 273-10 ~na.r . Ga l

do.

05-()9-79 32 18

7.4 8.6 3.6 180 150 7.6 3.1 .I

-

-

183

191 130 0

296 7. 7 22.8 5 18

50 2 I 2 0

240 2 10 (.5 0 350 10

do.

05-04-78 9 43

.4 1.7 .1 133 109 .8 3.0 .o 1.60

-

- 125 109 0 218 7.5

-0

- - ----

- - - -- - -

95-14 ~ 2 lff.lla_r Brev.i.ng Co.

do.

04-11-79 36 49

4.5 7.1 2.1 180 150 3.9 3.6 .I .oo .oo 199 195 140 0 304 7. 7 23.5 0

- 20 I 0 2 I

30 5 1 (.5 0 290 10

95-22 Al-baay-Doughi!n-y Co . , USMC Ocala

06-21-78 12

95-23 Morek and Co . lnc. 1

do.

08-D1-61 8

95-24 liectr- ~u rsery. 4

do.

08-09-57 10

95-03 USGs "Gl J.t A.lbany

do.

06-17-77 8

95-43 A.l:bau)', Ga ., 2.1

Mult1.aquiferl 06-18-70 34

95-37 .Ubo<ny, Ca . , 15

-

Pl!ia t. Jli.ver at: .U..,.ny

do.

06-23-76 24

Surface water 04-16-69 8

CSSTi

Cusseta

13

PVDC

Average values

Providence

12

50 50 45 45 40 16
7.3 5.2 1. 7

1.3 2.2 .5 7 2.0 .1
1.1 2.7 .3 .9 1.8 .2
6.1 17 2 . 7 6.0 42 5.7
.9 3. 7 1.8 1.6 622 3.8
.4 85 1.6

150 120 .2 3.5 .I 4.20

154 126 .4 2.0 .6 .70

140 115 1.0 147 120 .5 182 149 5.6 178 146 10
- 40 2.0

3.5 .3 6.10
- 2.6 .o

4.0 .4 . oo

6.0 .7 .oo

- 3.7

.10

903 746 4.0 422 3.3 .10

200 190 7.6 2.4 .6 .10

.00 158 148 130 7 239 7 .I 32.0 5 19 20 0 1 2 2

-

139

141 128 2

- - 244 7. 7 21.0 0 4.9

-

--

- - - 145 139 117 0 233 7. 7 24.0 4 4.5

-

--

- 131 132 120 0 234 7.4 21.5 5

- 10 I 0 0 0

I 3 10
-----
10 3 10

- .00 227 200 126 0 308 8.0 23 .0 5 2.9

10 - 0 0

10

- 197

- - - - - - 65 - 256 8.4

0

-

- 100

-

-

- 21 -

66 7.5 21.0 40

- - - - -

- 1,100

- .oo 1,505 I ,527 21 0 2,522

22.7 34 19 20 2 0 0 0

15

0 0 -0
- 50
1 15

- . oo 214 223 6 0 358

24.0 0 .2 40 0 3 1 0

50 10 0

( .5 0
---

80 10
--
--

.o 0 50 10

- - 320 -

-- - -
-- - -

<.5 0 395 5

<.5 0 - 0

CLTN TLLT

for each aquifer

Clayton Tallahattal/

20 12 34 40

5.0 44 3.0 159 128 12

2.5 .3 .10 . 00 175 174 49 0 258 - 22.9 6 26 26 I 1 0 0 152 6 10 <.5 0 336 0

6.6

9.6 2.8

181 165 6.5

3.9 . I .30 . 00

193

196 135 0

- 300

22.1 3 14

20 2 0 2 2

137 2 5 (.5 0 368 7

OCAL

Ocala
-

9.5 43 10

22

.3 148 120 .5 2.9 .3 3. 70 . 00 143 140 124 2 238 - 22.1 4 9.0 15 I 1 1 3

I 10 3 7 ( .5 0 65 10

1/ Georgia Environmental Protection Division standards for saf~ drinking water 1977.
2./ Ana lysis represents a composite of water from the Providence, Clayton, and Tallahatta aquifers. 3! Averages do not include analysis frow. site 273-QJ because of the proximity of well to recharge area . 4/ CSST - Cusseta Sand
- PVDC - Providence Sand
CLTN - Clayton For.ation TLLT - Tallahat.ta Formation OCAL - Ocala Limestone

8~3d

15'

8400'

3 1 45' .---------------~,-----~--------------------.-~--~~r---------~~~r---------~---------------------------r~-----,

('/

\

!~

CJ1

/ (> ~"''i'cb.
~,. 7 G>

.,:.("(t\ I' ,~.,:. 0 .. -,

G .. ...\

-z,. ...

3130'

//

//

\ r-'
~,~~~L-_~,
I
I
I
I

I

95-07 .(200)

~I

:~rII;It::
(!) 0

60 "'

I

J---

95- 11 (300)
- - - - - - ---D-O8U-AGHKEER-TRY --- -

Base from U. S.Geological Survey

1:24,000 quadrangles

0

- - - - - - - DOUGHERTY - - MITCHELL

5

10 MILES

EXPLANATION

1io8i - - 5 0 0 - - Ll NE OF EQUAL TRANSMISSIVITY--

DATA POINT- Top number is well identification.

Interval is 1000 and 2500 feet squared

Number in parentheses is estimated transmissivity

per day

in feet squared per day

Figure 7. Approximate transmissivity of the Clayton aquifer.

by the infiltration of rainfall. The Ocala is generally covered in the Dougherty Plain area by a thin layer of unconsolidated residuum ranging in thickness from about 40 to 70ft. Where the residuum is present, the aquifer is confined and is artesian; where the residuum has been removed by stream erosion or through sinkhole collapse, the aquifer is unconfined. Because of the varying conditions of confinement and pressure, average water levels in the Ocala during 1978 ranged areally from about 2ft above land surface to45 ft below.
Aquifer tests show that in areas near the Flint River where the Ocala Limestone is very cavernous, the transmissivity may exceed 100,000 ft 2/d (L. R. Hayes, oral commun., 1980). This high transmissivity allows the movement of large quantities of ground water, and yields to wells of 2,000 gal/min have been reported. However, away from the river in areas where solution openings are not well developed anc.J to the northwest where the aquifer is thinner, the transmissivity of the Ocala can be as low as 2,000 ft 1/d and wells are reported to produce about 500 gal/min .
Water from the Ocala aquifer is moderately hard and is classified as a calcium bicarbonate type (table 2). Water samples from wells 95-22, near the WorthDougherty County line, and 95-24, at the Herty Nursery in Albany, had higher concentrations of nitrate than samples from the underlying aquifers. Well 95-24 produced water having a nitrate concentration of 6.10 mg/L, the highest level detected in the report area. These anomously high nitrate concentrations probably are due to the leaching of soil which has been treated with nitrogen-base fertilizer.
Water from the Ocala generally is of good chemical quality and contains no constituent concentrations that exceed 1977 State drinking water standards. However, the quality of the water could change rapidly in areas where the aquifer is unconfined or is in direct contact with surface water.
Influence of the Flint River During periods of normal streamflow, the Ocal,l
aquifer discharges into the Flint River through cavernous zones in the limestone that have been exposed by stream erosion. Figures 8 and 9 are graphs showing precipitation and the stage of the Flint River at Albany during 1978. Comparison of these figures shows the effect of heavy rainfall on the Flint River. When the river stage is increased, ground water that normally discharges into the river backs up into the Jquifer, causing the water level to rise in Ocala wells near the river. Extended periods of he<1vy rainfall cause the river stage to rise above the altitude of the potentiometric surface in the Ocala aquifer. When this occurs, normal ground-water discharge points become re-

charge poi11ts and river Welter rJpidly enters the cavernous zones in the aquifer. Comporison of figure 10 with figure 9 shows th<Jt the W<lter level in well 95-03,4 mi southeast of Albany and e1bout 1.7 mi eJst of the Flint River, is very "flashy" and responds almost instantaneously to significant chJnges in river stc1ge. By contrast at well 95-22, near the Worth-Dougherty County line and about 5.1 mi from the river, the altitude of the potentiometric surface of the Ocala aquifer is higher than the maximum river stage, and the water level in this well (fig. 11) is less affected by the increased stage of the river.
Leakage
Although rainfall entering the aquifers where they occur near land surface is the primary source of recharge, another source of recharge exists in the Albany area. Pumpage that reduces the head, or artesian pressure, in an aquifer may promote increased vertical flow through the confining beds separating the pumped aquifer from aquifers of higher artesian pressure. The amount of leakage per unit area depends on three factors: (1) the vertical hydraulic conductivity of the confining layer; (2) the thickness of the confining layer; and (3) the head difference between the aquifers. In and near the city of Albany, heavy pumpage from the Providence, Clayton, and Tallahatta aquifers has produced head differences that could enhance leakage. Water-quality analyses indicate thJt water may be leaking from the Providence aquifer into the Clayton and from the Ocala aquifer into the Tallahatta. Additional test drilling and monitoring would be necessary to estimate the amount and areal extent of the leakage.
MULTIAQUIFER HYDROLOGY
When developed individually, the Providence, Clayton, and Tallahatta aquifers in the Albany area yield water to production wells in insufficient quanti-
ti to be o~l ffi 'iPnl. For thl re.t. on, the ity of
A l bany us w e ll that t, p two o r more aquifers im ult<~n u ly. Mult iaquifer w II ma ximi?e yi eld, anclq1inlmi7.e dr lwdown and dri ll ing cos t . T h ro u gh-
ou t nw h of th A l bany c1rea . prop erly onstructed
multiaquifer wells can produce a sustained yield greater than 1,500 gal / min and generate smaller drawdowns than wells tapping a single aquifer.
Well Construction
The telescoping construction design of two typical multiaquifer wells is shown in figure 12. Construction of each well is begun by drilling and driving a largediameter surface casing through the residuum. Drill-

16

4

I

I

I

I

I

I

I

I

I

I

I

- (f)
w 3

-

I

(.)

z

z

Albany-Dougherty County Airport weather station

z
0

2 -

r-

f<l: f-

-a...

(.)

w

a::

a... I--

i-

,I II I l 0 JAN.

I
FEB. MAR. I APR.

MAY

I~1 . 1I. -~

I

j II

I JUNE JULY

I AUG. SEPT. I OCT. I NOV.

DEC.

Figure 8. Daily precipitation at Albany-Dougherty County airport, 1978.

18 0~----~----~----~----~----~------~----~----~----~----~----~----~ (J)
C\J (J)

LL 175 0

U.S.Geologicol Survey station 02352500

w
6 165
Cil <l:

tJ 160
w
LL

z
- 155

w
(9

<l:

~ 150~----+-----+-----~-----+-----4------~----+-----~----~-----4----~----~

JAN .

DEC .

Figure 9. Mean daily stage of the Flint River at Albany, 1978.

17

w 25
0
it
0::
::::>
U)
0
z 30
<( _j
~
0
_j
w
!I)
f- 35 w
w
I.J..
z
w0:: ~
~ 45

JAN. FEB. MAR. APR. MAY

JUNE JULY

AUG. SEPT. OCT. NOV. DEC.

Figure 10. Daily water-level fluctuations in the Ocala aquifer at well 95-03, 4 miles southeast of Albany, 1978.

25
~ 0
_j
w
!I)
f-w Wl)
~it z-o.:~:
_jo
wz
><(
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0::
w
1--
<(
~
40

JAN.

APR. MAY

JUNE JULY

AUG. SEPT. OCT.

NOV.

DEC .

Figure 11. Daily water-level fluctuations in the Ocala aquifer at well 95-22, near the Worth-Dougherty County line, 1978.

18

TYPE I

t~~~~:.L: ::1 o 0
0 0
0
0 0

~ ~ ~ %
~ DO
.o
..0 0 0 0
D OC oO
" Jo 0 (
0 ~

0.

0 ,

0(1

0 01:1

00

~ ~

oo

0 0

0 0 0 0
"
Q "(
0 0
,o o
0 0 0
0 0 0
~
0 0
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Oo
0 0

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0 QD D
0
0 t
0 Oo
~
0
0 0
oo
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0 ()

,o

~ : 0

... 0 0 0 (

EXPLANATION

TYPE 2

~ SCREEN
V& CEMENT
I"o: "'Do ~C~', GRAVEL
TALLAHATTA AQUIFER

~ ~
~~ o.~~l 0 0 o' 0 Oo
0 0
0 0 0 0
0
OD
0
0
0 0
o
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D o
~

F:~~~~ II 0
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tJ 0
D 0
0 0
0 0
()
0
0
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oo
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OPEN HOLE-....\

r

CLAYTON AQUIFER

I
I
(

I I I

PROVIDENCE AQUIFER

~
oo r
Q._o 0

tH 0
_j 0 0 0 00

Figure 12. Typical multiaquifer well construction .

ing is then continued and another section of casing is installed thwugh the Ocala to prevent subsidence and to seal out water from the Ocala.
After drilling is completed to the desired depth in the type 1 well, the screen line is assembled above ground by welding alternating sections of blank casing and well screen at intervals corresponding to the water-bearing zones in the well. The assembled screen line is then positioned in the well and the space between the screen line and borehole wall is packed with coarse sand or gravel.
The second construction method (type 2 in fig. 12) is used in areas where the Clayton aquifer consists of competent limestone that does not require screening. In these wells, similar telescoping construction is used, except that in the Clayton Limestone the well bore is left as an open hole. A screen line, where utilized, is continued through the Providence aquifer.

The U.S. Geological Survey test wells drilled for this study (pl. 1) were constructed as single-aquifer wells, using either screened or open-hole construction. Wells tapping the Cusseta, Providence, and Tallahatta aquifers were screened to prevent the entry of sand. Because the Clayton and Ocala aquifers are composed of limestone, wells tapping these aquifers were not screened.
After completion, each well was developed to remove drilli1lg mud and fine sand from the well bore and adjacent aquifer material. Drillers emphasize this phase of well construction because well yield and aquifer response can be greatly increased if wells are properly developed.
Flow Through Idle Multiaquifer Wells
Brine-trace studies made in eight nonpumping production wells in and near the city of Albany

19

indicate that due to head differentials, a significant amount of ground water is transferred from the Providence and Tallahatta aquifers into the Clayton aquifer through idle multiaquifer wells. The brinetrace studies were done by injecting a concentrated sodium chloride solution into the boreholes at specified depths. Special geophysical sensors monitored the brine's velocity and direction of movement in the boreholes. Figure 13 shows the approximate velocity and the direction of flow measured in the boreholes of wells 95-33 and 95-34.
Recharge to the Clayton aquifer through well9533 was calculated to be about 12 gal/min, or 17,000 gal!d, from the Providence aquifer and about 46 gal/min, or 66,000 gal!d, from the Tallahatta aquifer. Thus, about 83,000 gal/d recharges the Clayton aquifer through this multiaquifer well. To approximate the

total recharge to the Clayton aquifer through idle wells, borehole velocities, based on brine-trace studies and well-construction data, were estimated for each multiaquifer city well. These velocities, together with pumping-frequency data, indicate that the 25 multiaquifer wells in the Albany water system recharge the Clayton aquifer at the rate of about 1.1 Mgal/d.
Areal Trends in Aquifer Yields
Flowmeter tests were conducted in six city supply wells to determine the relative percentage of water contributed by the Providence, Clayton, and Tallahatta aquifers to each multiaquifer well. The tests were done by first removing the turbine pump and pump column from the well and lowering a flowmeter, suspended by a thin steel cable, into the well.

95-33

EXPLANATION SCREEN

I d

I DIRECTION OF FLOW

95-34

TALLAHATTA AQUIFER

CLAYTON AQUIFER PROVIDENCE AQUIFER

I I OPEN......_I? I
HOLE

I I

t

ll

s t vi
..-fnln

J

Figure 13. Direction and velocity of flow in city of Albany wells 95-33 and 95-34 when wells were not pumping.
20

The pump assembly was then reinstalled and the well pumped at a constant rate until the water level in the well stabilized. The flowmeter was then traversed up the well to record the velocity of flow in the well bore at specified depths. By knowing the rate of discharge (gallons per minute), the diameter of the well bore (inches), the depth of each water-bearing zone (feet), and the me.Jsured velocity (feet per minute), the relative percentage of total discharge from the Providence, Clayton, and Tallahatta aquifers was calculated using the following equations:
Point discharge= Point velocity X diameter of well bore X 0.0408 (well constant),
then
Aquifer yield (percent)= Point discharge X 100. Total discharge
The flowmeter tests revealed that the percentage of total yield that each aquifer contributes to multiaquifer wells depends not only on the well construction and development but, more importantly, on the well location. Figures 14 and 15, constructed using flowmeter test data, show lines of equal yield for the Clayton and Tallahatta aquifers, respectively. In the east and southeast parts of the Albany area, the Providence and Clayton aquifers combined contribute less than 10 percent of the total yield of multiaquifer wells. In these areas the Tallahatta aquifer supplies the

remaining 90 percent of the well yield. However, in the west and northwest parts of the Albany area, the Providence and Clayton aquifers are more productive and at well 95-46, 2 mi west of Albany, each of the three aquifers contributes about one-third of the yield (figs. 14 and 15).
GROUND-WATER USE
According to Wait (1963), ground-water use in the Dougherty County area in 1957 was estimated to be about 8.94 Mgal/d. Since that time ground-water use has increased about 440 percent and is presently (1978) estimated to average about 39.4 Mgal/d (table 3).
Industrial
Due to the large number of new industries that have moved into the Albany area and to increased production at existing industries, water withdrawn from industrial wells has increased from about 1 Mgal/d in 1957 (Wait, 1963, p. 75) to the current (1978) pumpage of about 15.5 Mgal/d . Additionally, the city of Albany sells water to many industries that do not own wells. The latter pumpage is included in the municipal figures on table 3.
Ground water used for industrial purposes within the study area is obtained primarily from the Ocala aquifer (table 3).

Table 3.

Estimated ground-water use in the Albany area, 1978.

Aquifer

Ground-water use (Mgal/ d)

Agricultural.!/ Industrial

Municipal

Total

Providence

--

--

0.9

0.9

Clayton Tallahatta Ocala

0.5
.5
-
7.9

0.5
--
15.0

6.8

7.8

7.3

7.8

-

22.9

TOTAL

8.9

15.5

15.0

39.4

1/ Values are estimated growing-season withdrawals averaged over a 365-day peri0cl.
21

TERRELL

r-.) r-.)
3130'

EXPLANATION
LINE OF APPROXIMATE EQUAL YIELD-Interval 20 percent
95-47
e DATA POl NT- Number is well
identification number
AQUIFER YIELD-In percent as follows:
~ Providence aquifer Clayton aquifer Tallahotta aquifer

Base from U.S. Geological Survey

0

I : 24,000 quadrangles

DOUGHERTY ~CHE~-

5

10 MILES

Figure 14. Results of flowmeter tests and the percentage of multiaquifer well yield from the Clayton aquifer.

TERRELL DOUGHERTY

iw'J

,_fl.
t ~
~
()
&

Bose from U.S. Geological Survey

0

I: 24,000 quadrangles

EXPLANATION
- 2 0 - LINE OF APPROXIMATE EQUAL
YIELD-Interval 20 percent
95-47
e DATA POl NT- Number is well
identification number

AQUIFER YIELD-In percent as follows:



~ Providence aquifer Clayton aquifer Tallahatta aquifer

DOUGHERTY
Mi"'f"CHE~ -

5

10 MILES

Figure 15. Results of flowmeter tests and the percentage of multiaquifer well yield from the Tallahatta aquifer.

Agricultural
Total irrigated cropland in the study area reported in the 1954 agricultural census was 200 acres. By 1978 the irrigated cropland had increased to about 8,650 acres. According to Pollard and others (1978), ground water represented about 92 percent of the water used for irrigation in 1977 and it is assumed that this percentage did not ch<mge appreciably for the 1978 crop season. Thus, during 1978 about 8,000 acres were irrigated by ground water.
The availability of suffici ent ground water and the suitability of center-pivot systems has greatly enhanced the use of irrigation in the Albany area. The gentle slopes and large fields permit the use of selfpropelled center-pivot irrigation systems. Many center-pivot systems used in the study area are designed to distribute water at rates of 1,000 to 1,500 gal/min and are capable of irrigating several hundred acres.
Ground water for irrigation in the Dougherty Plain province is obtained primarily from the Ocala aquifer. However, the Ocala is not produdive to the northwest of Albany in parts of Dougherty. Terrell, and Calhoun Counties, and use of the Clayton aquifer for irrigation is rapidly increasing . Agricultural use of ground water is presently (1978) not regulated by the State of Georgia. Because permitting is not required, agricultural use of the Clayton is limited only by the productivity of the aquifer. Heavy withdrawals from the Clayton in this area could limit the availability of water from this aquifer.

5500
0:::
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w>-
0:::
w
Q.
5000
(f)
z
g
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Q.

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-

-

r--

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~

4000

-'

69 70 7 I 72 73 74 75 76 77 78

1969-78

Figure 16. Yearly ground-water withdraw.al by Albany supply wells, 1969-78.

Municipal
In 1898 the city of Albany's water system pumped an estimated 25,000 gal / d from 14 wells (McCallie, 1898, p.179-181).As municipal and industrial demands increased, more wells were drilled, and the city has used at least 30 wells since initiation of the Albany

withdrawals from April through October 1978. The duration of peak withdrawal periods and the amounts of withdrawal are influenced by climatic conditions; thus, increases in precipitation decrease the demand for city water.

water system. The city of Albany was the largest single ground-water user in the study area during 1978, withdrawing a total of about 5.4 billion gallons per

Municipal Pumpage from the Providence, Clayton, and Tallahatta Aquifers

year, from 23 multiaquifer wells (fig. 16). The increase in population and industry in the

The total amount of water withdrawn from the Providence, Clayton, and Tallahatta aquifers was

Albany area is reflected in the water requirements. Figure 16 shows that the annual ground-water demand

estimated for the Albany supply wells based on flowmeter tests and well construction data. Figure 18

has increased from about 4.2 billion gallons in 1969 to

shows that an average of about 0.9 Mgal/d was

more than 5.4 billion gallons in 1978. On August 28, 1978, the ground-water withdrawal peaked at over 22

withdrawn from the Providence aquifer during 1978, or about 6 percent of the Albany municipal supply.

Mgal/d, the highest single day of pumpage recorded by the city of Albany (fig. 17).
The rate of ground-water withdrawal by the city

The Clayton aquifer contributed about 45 percent of the city supply, or an average of about 6.8 Mgal/d . Approximately 7.3 Mgal/d was withdrawn from the

varies seasonally and is greatest during the summer

Tallahatta aquifer during 1978, representing about 49

and fall. Figure 17 shows an increase in ground water

percent of the total Albany municipal pumpage.

.-

24

(/)
z
0 ...J ...J
(5

z

I o>-
:::i(3

AVERAGE

...J 16
~5 - - - - - - - - - -

zO..

/August 28,1978

Figure 17. Total daily ground-water withdrawal by Albany supply wells, 1978.

GROUND-WATER LEVELS
Potentiometric Surface Characteristics
The altitude pf the potentiom etric surface of an aquifer is highest in recharge ar eas. Ground water flows laterally down gradient from the recharge areas, in a direction perpendicular to the potentiometric coutour lines, to discharge ar ea s where the potentiometric surface is lower. Wh e n discharge exceeds recharge, the potenti'ometricsurface will be depressed.
Clayton Aquifer
During the period of September4-6, 1979.21 wells tapping th e Clayton aquifer w ere measured to obtain data for constructing a pot entiometric map (pl. 1). Th e c losed contours on th e Clayton potentiometic surface in the Albany area define a pumpage cone resulting from many years of heavy ground-water withdr awal. Increased agricultural pumpage in the northwest part of the study ar ea has also depressed the potentiometric surface of the Clayton there, and has caus ed the pumpage con e at Albany to elongate about 14 mi in that direction . The potentiometri c contour lines indicate that the primary direction of ground-water flow in the Clayton aquifer is toward th e area of greatest withdrawal, which at present is the city of Albany.
Tallahatta Aquifer
Water-level measurements were made in 14 wells tapping the Tallahatta aquifer, concurrently with measurements in the Clayton wells . From plate 1 it can be seen that the potentiometric surface of the Tallahatta aquifer is not depressed as deeply as that of the Clayton; however, the broad areal extent of the

pumpage cone refl ects th e stress placed on the aquifer. The southw est elongation of the pumpage cone probably is a function of the water-bearing characteristics of the Tallahatta aquifer rather than of stress. Additional hydrologi c testing in the southwest part of the report area could better define the pumpage cone. The indicated direction of ground-water flow in the Tallahatta aquifer is toward the city of Albany.
Ocala Aquifer
A potentiometric map of the Ocala aquifer was constructed from measurem ents made in November 1979 (fig. 19). The potentiom etric contours indi cate that the aquifer receives recharge throughout much of the report area and dis c harges through springs and into streams where erosion has removed the confining layer. Abundant local ~echarge has prevented the development of widespread pumpage cones in the Ocala potentiometric surfa ce.
Long-Term Water-Level Declines
Records indicate that ground-water levels in the Providence, Clayton, and Tallahatta aquifers have been declining in the Albany area since 1898 and probably before (McCallie, 1898, p. 180). During the 1800's, ground-water withdrawals were small and natural recharge probably maintained a state of water-level equilibrium in the aquifers. As groundwater demand increased, recharge no longer kept pace with withdrawals and ground water began to be mined from aquifer storage, resulting in declining water levels.
According to records maintained by drilling contractors, wells tapping the Providence aquifer flowed

25

>-
<(
Cl
0::: 8 w
a_
(/)
z
0
_J
_J 6
<( C)
z
0
_J _J
~ 4
z
uS
C) <(
a_
~ 2
::::::> a_

EXPLANATION

-

PROVIDENCE AQUIFER

t8881 CLAYTON AQUIFER

~~\.~\.\\;] TALLAHATTA AQUIFER

Figure 18. Estimated monthly mean pumpage by the city of Albany from the Providence, Clayton, and Tallahatta aquifers, 1978.

during the early 1900's. Heavy municipal and industrial pumpage have lowered ground-water levels, and wells in this aquifer no longer flow. Since 1940, ground-water levels in the Providence aquifer have declined as much as 100 ft in the Albany area (R.E. Faye, oral commun., 1980).
Before 1940, artesian pressure in the Clayton aquifer was sufficient to produce many flowing wells. However, heavy municipal and agricultural pumpage has lowered water levels in the Clayton aquifer, near the center of pumpage at Albany, more than 135 ft

and wells no longer flow. Figure 20 shows how increased city pumpage since 1975 has resulted in a declining trend in the water level in well 95-09 near Albany. The water level in this well has declined about 25 ft si nee 1975.
Few single-aquifer wells penetrated the Tallahatta prior to 1960 and historical water-level data are minimal. However, water levels in the Tallahatta aquifer probably have declined significantly since 1940 in the Albany area. Water levels in the Tallahatta aquifer at well177-07, about 10 mi north of Albany at Leesburg,

26

r

tv -...!

EXPLANATION
-/70-POTENTIOMETRIC CONTOURShows appro~imate altitude at which water would have stood in tightly cased wells . Contour interval 10 feet. Nationa I geodetic vertical datum of 1929
147
e DATA POINT -Number Is appro..l ma t e alt i tude o f pot ent iometr ic surface i n feet

Bose from U.S. Geological Survey

0

I: 24,000 quadrangles

DOUGHERTY
""""""M!TCHE~ -

5

10 MILES Hydrology from G.D.Mitchel1,1979

Figure 19. Potentiometric surface of the Ocala aquifer in the Albany area, November 1979.

40
u w
Lt 50
a::
::::>
(/)
0z 60 -
<t:
_J
3:
0
_J
w
a:l
Iwwu.-.. z
_j
w
w >
_J
wa::
I-
<t:
~ 120
1970

AVERAGE DAILY PUMPAGE--._ AVERAGE WATER LEVELS~

18

16

>-
<t:

0

a::
14 wa..

(/)
z

12

0
_J

-'

_J

<t:
(.!)

10 z
0
_J _J

8 :E
z
w
6 (.!) a<.t.: :E ::::>
4 a..

2
1978

Figure 20. Average daily pumpage from Albany supply wells, 1974-78, and average water-level

fluctuations

in

th. e

Cla-yton

aquifer

at

well
.

95-09

near

Albany,

1970-78.

have declined about 15 ft since 1940. Therefore,
because ground-water withdrawals in Albany are significantly larger than at Leesburg, it can be assumed that water-level declines in the Tallahatta at Albany have been greater.
Seasonal Fluctuations In Ground-Water Levels
Ground-water levels in the study area fluctuate in response to seasonal variations in precipitation, streamflow, evapotranspiration, and pumpage. Figure 8, 9, and 10 compare precipitation data collected at the Albany-Dougherty County airport with streamflow recorded at the U .S. Geological Survey gage on the Flint River at Albany and water levels in the Ocala aquifer at wells 95-03, 4 mi south east of Albany, and 95-22, near the Worth-Dougherty Countyline . Abundant winter rainfall increases th e potential for recharge of the Ocala aquifer throughout the area. During the winter months, when vegetation growth and solar radiation are at a minimum, evapotranspiration is low and the aquifer re ceives the maximum annual recharge. Accordingly, water level s in the Ocala aquifer recover from the previous year's minimum by early spring. Although precipitation is generally heavy from April through September, water lost to evapotranspiration is greatest during the growing season

and the amount of water available for recharge is reduced. Thus, reduced re charge and increased agricultural pumpage during th e spring and summer seasons cause ground-water levels in the Ocala to decline to a minimum by late fall.
Because the Clayton and Tallahatta aquifers are re charged 20 to 40 mi north and northeast of the Albany area , wat er levels in th ese aquifers are affected primarily by changes in local pumpage. During November through March, a 3.3 Mgal/d decrease in municipal pumpage (fig. 17), and a substantial decrease in agricultural pumpage during this period, results in a reduction in total ground-water withdrawal. Due to this reduced pumpage, and a slight increase in recharge, ground-water levels in the Clayton and Tallahatta aquifers attain a maximum by late winter (figs. 21 and 22) . During the spring and summer , increased municipal and agricultural pumpage causes water levels to decline to a minimum by late fall.
CONCLUSIONS AND SUGGESTIONS
Ground water in the Alb any area is obtained from four aquifers. From deepest to shallowest the aquifers are: the Provid ence, the Clayton, the Tallahatta, and the Ocala. Although ground water is available from the underlying Cusseta, high drilling costs, low yields, and excessive concentrations of chloride and dissolved solids make development of this unit undesirable.

28

g3::
w
(Il

~ t5 130
W<[ lLlL
z~
-(/)
w_rzo ~ :51 4 0
_j

0w::
1-
<(
3::

150 L_~~~~~~~_L--___j_____~____L_____L___~----~----~~--~--~

JAN.

JUNE JULY AUG. SEPT. OCT. NOV. DEC .

Figure 21. Daily water-level fluctuations in the Clayton aquifer at well 95-06 at Albany, 1978.

3::
0
_j
w
(Il
t;J t5 80
~~
zo::
-~~
W _ j o z
~ :5 90
_j
0::
w
1-
<(
3::

APR. MAY

JUNE JULY

AUG . SEPT. OCT.

NOV. DEC.

Figure 22. Daily water-level fluctuations in the Tallahatta aquifer at well 95-05 at Albany, 1978.

Providence Aquifer
Water from the Providence coquina and sand aquifer is obtained at depths ranging from about 640 to 960ft below land surface. The Providence dips to the southeast at about 23 ft/mi and progressively thickens in that direction.
The aquifer is confined from below by the clayey Ripley Formation and from above by the silty upper Providence-lower Clayton sequence. Water levels in the Providence during 1978 averaged about 110 ft below land surface near the center of pumpage in Albany.

Transmissivity estimates for the Providence aquifer range from about 250 ft 2/ d in the southeast part of the area to about 1,000 ft 2/d updip in the northwest. In the south and southeast, wells produce less than 25 gal/min; however, updip to the northwest, yields to wells of about 500 gal/min have been reported. Throughout the report area pumpage from the Providence generates large drawdowns due to the low transmissivity of the aquifer, especially in the southeast.
The Providence yields a soft sodium bicarbonate type water that contains no concentrations of constit-

29

uents that exceed the State standards (1977) for drinking water.
Water from the Providence is used chiefly for municipal supplies in the Albany area, where an average of 0.9 Mgal/d was withdrawn during 1978. Withdrawals from the aquifer have caused water levels to decline about 100ft since 1940.
Clayton Aquifer
Water is obtained from the limestone part of the Clayton Formation at depths ranging from 550 to 840 ft below land surface. The limestone part of the Clayton ranges in thickness from about 70ft downdip to the southea.st to about 125ft to the northwest.
The aquifer is confined from below by the silty upper Providence-lower Clayton sequence and from above by the clayey Tuscahoma Sand. Measurements made during 1978 revealed that water levels in the Clayton were the lowest in the Albany area, averaging about 140 ft below land surface in well 95-06 at Albany, near the center of pumpage.
At well95-09, 3 mi east of Albany, the transmissivity of the Clayton aquifer is about 400 ftl/d and well yields average about 250 gal/min. However, to the northwest near Sasser, the transmissivity of the Clayton aquifer is about 11,000 ftl/d and yields to wells of about 2,000 gal/min have been reported. The progressive increase in transmissivity and yield to the northwest is due largely to thickening of the aquifer and a directional increase in hydraulic conductivity.
The Clayton aquifer produces a soft sodium bicarbonate water that is suitable for most uses and contains no constituent concentrations that exceed State standards (1977) for drinking water. The average sodium concentration of 44 mg/L is uncharacteristically high for a carbonate aquifer and could result from leakage of sodium bicarbonate water from the Providence aquifer through an intervening confining layer into the Clayton.
Brine-trace studies indicate that in the Albany area about 1.1 Mgal/d is being artificially recharged to the Clayton, through idle multiaquifer wells, from the Providence and Tallahatta aquifers of higher head.
An average of about 7.8 Mgal/d was withdrawn from the Clayton aquifer during 1978 for municipal, industrial, and agricultural supplies in the Albany area. Heavy withdrawals have resulted in a waterlevel decline near the Albany pumping center of about 135ft since 1940. Increased municipal pumpage of about 3.0 Mgal/d since 1975 has lowered water levels in the Clayton aquifer about 25 ft at well 95-09 near Albany. Accelerated agricultural use of the Clayton to the west and nor.thwest in parts of Dougherty, Terrell, and Calhoun Counties has produced signifi-

cant water-level declines in that area and could limit the availability of water from this aquifer.
Tallahatta Aquifer
The Tallahatta aquifer underlies the report area at depths of 125 to 350ft below land surface. The aquifer dips to the southeast at about 12 ft/mi and thickens in that direction.
The Tallahatta is confined from below by the clayey Tuscahoma Sand and from above by part of the Lisbon Formation. Water levels during 1978 at well 95-05 in Albany averaged about 90 ft below land surface.
Estimates of transmissivity range from 2,400 to 3,500 ft 2/d and reported yields to wells range from about 1,000 to 1,400 gal/min. However, withdrawal rates great'er than about 750 gal/min produce large drawdowns.
Water from the Tallahatta is a hard calcium bicarbonate type and contains no concentrations of constituents that exceed the Georgia Environmental Protection Division standards (1977) for safe drinking water. The average dissolved calcium concentration of 40 mg/L is uncharacteristically high for a predominantly sand aquifer and could result from vertical leakage of water from the Ocala through the intervening Lisbon Formation.
During 1978 an average of 7.8 Mgal/d was withdrawn from the Tallahatta aquifer for agricultural, municipal, and industrial supplies in the Albany area. Long-term withdrawal in the Albany area has caused water levels in the Tallahatta to decline, probably as much as 40ft near the center of pumpage.
Ocala AQuifer
Water can be obtained from the Ocala aquifer throughout the Dougherty Plain part of the report area at depths ranging from about 40 to 70ft below land surface.
The Ocala aquifer is unconfined where stream erosion has exposed the limestone and in areas of sinkhole development. Elsewhere, the aquifer is confined from below by the Lisbon Formation and from above by 40 to 70ft of residuum. Because of the varying conditions of confinement, average water levels in the Ocala during 1978 ranged areally from about 2ft above to 45ft below land surface.
In areas near the Flint River where the Ocala is cavernous, transmissivities exceed 100,000 ft 2/d and wells tapping the aquifer are reported to produce as much as 2,000 gal/min with minimal drawdowns. In
other areas the transmissivities are as low as 2,000 ft 2/d
and yields to wells may be as low as 500 gal/min.

30

Water from the OcJiil generc1lly is of good quality and contains no concentrations of co nstituell ts that exceed Stdte drinking water standards: however, in areJs wher(' the Jquifer is poorly con fined and in di1ect contact with surface wJter, the quJiity could rJpidly Lhange.
An average of 22.9 Mgal/d wa s withdrawn from the Ocala dquifer in 1978 for industrial and Jgricultural supply in the Albany area. Be cause of abundant local recharge, no long-term water-level declines have be en observed.
Suggestions
A supply of good quality ground water is presently .1vailabl e in the report area. The following considerations could h e lp evaluc1t e the effects of future groundwater development in the area, prolong the produ ctivity of th e aquifers, and protect the quality of the ground water.
1. Due to the low productivity of the Providence and Clayton aquifers in the east and south east parts of the repo rt area, the development of supply wells tapping only the T,dlahatta aquifer could produce yields comparable to multiaqu ifer wells and cut construction costs.
2. To reduce lo ca l Jrawdown, supply wells could be spaced over a larger area. Testing indicates that multiaquifer wells developed i11 the northwest part of the report area produce good yields with relatively small drawdowns.
3. The development potential of the Ocala aquifer could be considered in areas wher e the aquifer is confined and is not in direct contact with surface water. The high yield and normal good quality of water from the Ocala rnake it a viable water source i11 mc1ny areas.
4. Because artesian pressure is lower in the Providence aquifer than in the underlying water-bearing units, wells that penetrate the co nfining Ripley Formation should be sedled subsequent to testing and sampling to prohibit th e upward movement of poor-quality water.
SELECTED REFERENCES
Clark, W. Z., Jr., and Zisa, A. C., 1976, Physiographic map of Georgia: Georgia Dept. Natural Resour ces, Geologic and Water Resources Div., 1:2,000,000 .
Cooke, C. W., 1943, Geology of the Coastal Plain of Georgia: U.S. Geol. Survey Bull. 941, p.121, pl.1.
Georgia Geological Survey, 1976, Geologic rnap of Georgia, 1:500,000.
Georgia Environmental Protection Division, 1977, Rules for safe drinking water: Chap. 391-3-5,57 p .

Hem, J. D., 1970, Study and interpretation of the c hemical characteristics of natural water: U.S. Geol. Survey Water-Supply Paper 1473 , p. 54-150.
Herri ck , S.M., 1961, Well logs of the Coastal Plain of G eo rgia: Georgia Geol. Survey Bull. 70, p. 170-181.
Krause, R. E., 1978, Geohydrology of Brooks, Lowndes, and western Echols Counti es, Georgia: U.S. Geol. Survey Water-Resources lnv. Open-File Rept. 78117, 82 p.
LaForg e, Laurence, Cook, Wyth e, Keith, Arthur, and Campbell, M . R., 1925, Physical geography of Georgia: Geol. Survey G eo rgia Bull. 42, 189 p.
Lohman, S. W., 1972, Ground-water hydrauli cs: U.S. Geol. Survey Prof. Paper 708, 70 p .
McCalli e, S. W., 1898, A preliminary report on the artesian-well system of Georgia: Georgia Geol. Survey Bull. 7, p. 63-64, 177-183 .
Mit c hell, G. D ., 1980, Potentiom etric surface of the principal artesian aquifer in Gerogia, 1979; U.S. Geol. Survey Open-File Rept. 80-585, scale 1:500,000,1 sheet.
Owen. Vaux, Jr., 1958, Summary of ground-water resources of Lee County, Georgia: Georgia Geol. Survey Min. Newsletter , v. 11, no. 4, p. 118-121.
___1963, Geology and ground-water resour ces of Lee and Sumt er Counties, southwest Georgia: U.S. Geol. Surv ey Water-Supply Paper 1666,70 p.
Pollard, L. D., Grantham, R. G., and Blanchard, H. E., Jr ., 1978, A preliminary appraisal of the impact of agriculture on ground-water availability in southwest Georgia: U.S. Geol. Survey Water-R eso urces lnv. 79-7, 21 p.
Stephenson, L. W., and Veatch , V. 0., 1915, Underground waters of the Coastal Plain of Georgia, and a discussion of The quality of the waters, by R. B. Dole: U.S. Geol. Survey Water-Supply Paper 341,539p.
Stringfi eld, V. T., 1966, Artesian water in Tertiary limestone in th e Southeastern States: U.S. Geol. Survey Prof. Pap er 517, 134 p.
U.S. Environmental Protection Agency, 1977, National interim primary drinking water regulations: EPA570/9-76-003, 159 p.
Wait, R. L., 1960, Source and quality of ground water in southwestern Georgia: Georgia Geol. Survey Info. Circ. 18,74 p.
-,--1963, Geology and ground-water resources of Dougherty County, Georgia: U.S. Geol. Survey Water-Supply Paper 1539-P, 102 p.

31

Pr epared in cooperat i on with the

GEORGIA DEPARTMEN T OF NAT URAL RESOURC ES

DEPAR T MENT OF THE INTERIOR

I NFORMATION CIRCULAR 57

GEORGI A GEOLOGIC SU RV EY

U. S. GEO L OG I CA L SURVEY

PLATE I

31"45' 31"45'8~4~3-0-' ------,---------------r-------------~~r.---------~--------------------------------2~0-' -------------------~----~~----~------~r-----------~----------------------~-------i----r------------,------------------------~=5-' ---------------------------------------8-4~"~00~'----------------------------------------8~3'~55'

()

"2 '

-<

17 7 - 0 8 ( 1 8 2 )

::0 l>
r

D
r-7
'1 )
-- -- ...___
c'?

' \.._s- roc~ Ksl
\\.POfr(J ( vV

Well number

Well identifiClltion

Own er'~ name

Date dri lled

Aquifer

Construr.tion

37~ 1
31 -02
.....,, ,95-01
95.02
!liS -OS 95.()6

31353008<1282701
3311.ll,2.6,0.,8.4,2.9,.4.1,0.1,
J13lOS08406430'1 313105064064302 J13S301J8.420320l J1l53406410l001
31)5~ 1 03002 31310~202
31353408-4103001 JllSS4034062501
Jl~S.f06.42 1 01 0l J126S)3.421010 3 312654064210101

Graham, E.R.. 2 Adams, C., 2 USGS TW1, Albany
USGS lW2, Alb.any USGS TWJ, Alb.any USGS lW.C, Albany
USGS TWS, Albany uses TW6, Albany USGS TWl, Albany uses TW10, Alb<lny
Turner C itv, 2 DNR TW1 1, Al ban ~
DNII. TW12, Albany S!!aly,j.R., 2

,,,,,,,.,,,,,,,.
1976

sao
500
,,1,-47<1 418
"'257 """'1,346

...<70 C la)'IOI'I do.

1,47<1 Cus!eta

418 Tallahau a

54 Ocala

"' Tallahatta

257

do.

,,..619 Clayton

716

do ..

19"
' "9 1979 ' 1978

"""'"'' ,. 1,200

713
630 1 .100

Open hole do
Saeened do.
Open hole
Scr~n ed
do. Open hole
do. Screen ed
Open hole Screened
Open hole do.

10

25 0

u

30

95-14
9515 95 -16 95-17

31352 7~1
31l55108404.f001 J136090a404JS01 31352701W045201 31354SQ6.40oW701

P'N l , Mi ller Brew ing Co. PW2. Mi ller Brewing Co. PWJ, M i ller Brewing Co. OWl , M iller Brew ing to. OW2, Miller lllew ing Co.

"'''1""9"7"'''9

942 560 550 942 560

942

560

550

942 560

' T~ll ~ h a t t~

Screened do.
do. do. do.

1,599

1) . 7

1 ~04

9.1

1 ,370

7.0

95 -18 )1~1 OWJ, M iller Brew ing Co.

1979

550

550

do.

do.

9519 95-20 95 -21 95-22 95-23
952 ~ 95- 25
95-26 9 5 - 27
9S-28 9S -' l 9 95- 30 95 - 31 95-32 95-33 95-34 95- 35

J13551Q&404.4001 J 1360908.4005{12 3136250&4041501
3137~290 1
3129511034074601 3132-46084105601 31l530IJIJ42032D1 31300700416-4801 3127-'f1084010801
31345-40&4083801 3134084090301 J1J+f90&4085901 3134)6()84()81801 31345201W093901 313455083102501 313525064111401 3134-45084092201

USGS OWl, M iller Brewing Co. USGS OW3, Miller Brewing Co. firewe ii-SAC A~on, Miller Brewing Co. Albllny-Dousherly Co., U.S. Marine Corps Merck and Co., lrn:., 1 Hert}' Nu rse ry, 4 TaiiJhass~ Pl antation, DNR St. Joe Paper Co. , ~rnett Well Ba rlow, D.
Al~ny,6
AIU...ny, 7 Albany . 8
Alba ny, 9 Albany ,10 Alba ny, 11 A lb a n y , 1 2 A lb~ ny. 13

1979
,,..' "9
1979
"'1"97"'3
1942
.., ,1937
1939
1947
, ,1949
1952 1952

""35''0
" '247
""79''5
442
955 1 .022
""868'' "72S'
800

60 60 350
""80 69 542
..,542
442
,.,
653 695
""915 '"676

Oc~li
do.
T<~llih a na Ocala
do. do. C layto n Cr e tac eous Tallahalta
I I
do. do. do. do. do. do.

Open hole do .
Screened
O pen hole do. do do do
Scre,.ned
Screened and open hole
do do. do. do.
Scre~rted Screened ~nd o pen hole
do.

465
1,083 700
1,677 1,258 1,415
"'"'870

11.3
6.9
8 . 12.4 13.9
5.8
7'.7'

95-36 3134290!Wl12301 Alba nv, 14

1954

855

855

do.

do.

699

SA

95 -37 95-lll

31361006--1105001 A lb~ n v . 15 3135500640!13001 Alba nv, 16

1954 1955

895 865

'"865

do. do.

do. do.

1.318

12.3

1,03>1

8.0

95 -19 95-411 95-41
95-42 95-tJ 95 . . . 9S -4S 95-46 95-47 95-48 95-49

31355506-4062601 3136Z1064122801 31341-408-4060301
3 1 325~101
313147084072201 313403064130101 313702084113101 313507064132801 31342110114044901 31355-4084143901 313650084122901

A l b~ny, 1 7 A l b~ n y, 18 Albany, 19 Alba ny, 20 Albany. 21
Albany. 22 Albany, 23 Albany. 24 Albany, 25
Albany. 26 Albany, 27

1951

470

470 hllaha lu

,.,1960 "'1"""9"""70'

855
'""8'9""1'''
840
890

855
"'""'' .000 891 840 890

I do. do. do. do do. do.

19n
1973
197&

955
"'820

" '820

do. do.

$20

do.

Screened
Scre~ nen a nd open ho le
do. do. Screened
do. do. do. do do. do.

"'1,092

9.2 9.7

1,272

1].8

556

6.4

t,:Wl

6.2

1,102

5.9

1,116

19.1

1,300

11.7

1,])6

10.7

1,500

13.2

1,404

16.7

95-50 95-51 95-52

313&15084055001 3135190113594901 31J.6084065701

Albany, 28 Albany, 29 Albany, 30

,"", ... 1977

1,010 1.178

1.010 1 ,178
940

do. do. do.

do. do. do.

1,500

1,529

9.5

1,500

11.5

95-53 313252084022201 U.S. Ma rine Co rps, 2

1952

997

997

do.

Screened and open hole

1,700

13.9

95-54 95-55 95-56 95 57 177- 01

3132418406 1101 31315-40842-44101 313425084192301
3133<4908-4100601 3138130841 25001

U.S. Ma rin e Corps, 3
Fori, ].1' Grah ~ m,E.R ., 1
Vi rginia-Caro li na Chemical Co. U~G S TWS, Alb.an y

1954 1881 19 1 1 1918 1 976

""'547 '"594
)85

900

do.

,..,
.,,

C lay1on do. do.
Ta lla halta

do. O peo hole
do. do. Screened

1,5 15

9.9

177-(12 177-03 177-04 177-05 177-06

313612004125001 314237004103601 313Sl9084103601 31380101:141 05001 Jl-4002064122801 314353064 10020 1 314150084131601 314010084172501 314030084171701 314012084180-401 314118084190901 31431308-4205801 314413064242401

USGS TW9, A l ban~ Winl!,fieid, J. Leer.is h Acre~, 1 Leehig h Acre!i, 2 Fow llown Plan1ation Lce!ibu rg, 3
Haley Brothers Fa rm Fryer ,W.H. Lilliston lmplemenl Co. Piedmont Plomt Farm O~ niel Brothers, 2
Sasser,] Brown's Dairy

1976 1952 1971 1973

..."'700
675

567 C layton

555

Pro~i dence

555 Clayton

560

do.

Open hole do. do. do.

1938
1957 1967

"'320
...300
213
'"J20

560

do.

"" hllahaHa do.

,HJ
520

d~ C lay~ on
do.

320 Tallaha lta

do. Screened
Open hole do. do.
do.
Scrte~d

.6,2.0

475 Cla)'lon

394

do

Open hole do.

200

572

9.7

"'18"'0

13.3 20.5

"'656

19.9

7.5

350

38.9

314322064231601 Locke. B.

1979

530

<20

do

do.

2.000

28.0

314127084234701 Dan iel Brothers,)

540

430

do.

do.

31-40530&4233601 Wk i n ;~ker, B., 2

545

<25

do.

do.

314132084255501 Reese, S.

200

200 Ta llaha tta

Saeened

313856084295501 BanKS, J.

500

<00 Claylon

Open hole

31431408-4205701 Sasser, 2

202

202 T~ll aha lta

Screened

3144020114215901 W hittake r, B., 1

520

400 Clayton

Open hole

I
I
I

I I f
I

I

95-51

35'

95- 54

95- 55

I

0

~~I

W IIiO::

6 5 < . 9 0

0

EXPLANAT I ON

- 1 5 0 - - POTEN T IOME T RIC CONTO UR - Shows a l titude at which water leve l wou ld
have stood in tig htly cased wel l s topp i ng t he Cla yton aq ui fer. Das hed where o.pproximate ly located . Cont ou r i nterva l 25 feet. Nat i ona l geodet i c vertica l datum of 1929
- - - 100- - POTENTIOM ETRIC CONTOUR - Shows altitude of whic h water level wou l d
hove stood in tight ly cased wells tapping t he Tal l ahatta aqu ifer. Dashed where approximately l ocated. Contour interva l 50 feel. Notional geodetic vert i cal datum of 1929

A - - - - A ' GEOLOG I C SECTION

95- ll (l56)o DATA POINT -- Number outs ide pa r ent hesis is we l l ident i fica t ion. Number 95-10(1 57Je insi de parenthesis i s alt i tude of poten ti omet r ic su rf ace i n feet

WE LL IDENT I FI CATION BY AQU IFER
e Cre ta ceous

0

Cl ayton Tallaho tt a

() Oca la

Multi aquifer

. J - - - 15 0_J.-

+

95-27(186)

I
L__ _l
___ j '

Base ho m U.S. Geolog ical Su rvey 1, 24,000 Quadra n g le s

2

15 '

10

s'

OErErErEr~J=========~2==========3E=========r4=========J5M I LES

POTENTIOMETRIC SURFACES OF THE CLAYTON AND TALLAHATTA AQUIFERS AND WELL LOCATIONS IN THE ALBANY AREA, GEORGIA, SEPTEMBER

1979.



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