THE WARM SPRINGS OF GEORGIA

UNITED

STATES

DEPARTMENT

OF

THE

INTERIOR

Harold

L.

Ickes,

Secretary

GEOLOGICAL

SURVEY

W.

C.

Mendenhall,

Director

Water-Supply

Paper

819

THE

WARM

SPRINGS

OF

GEORGIA

THEIR

GEOLOGIC

RELATIONS

AND

ORIGIN

RY

REPORT

D.

F.

HEWT«NDOG.

W.

CRICKMAY

V

»

**t*

Prepared

in

cqope?ktio^^lh

the

GEORGIA

DEPARTipSff

OFJiipRESTRY

AND

UNITED

STATES

GOVERNMENT

PRINTING

OFFICE

WASHINGTON

:

1937

For

sale

by

theJBuperintendent

of

Documents,

Washington,

D.

C.

Price

25

cents

CONTENTS

Page

Abstract

_________________________________________________________

1

Introduction

______________________________________________________

1

Scope

of

the

investigation._________________________________________

2

Acknowledgments-

________________________________________________

2

Surface

features.___--_------___-_-___________.________-_--_____-__

2

Warm

springs

of

the

region_________________________________________

3

Warm

Springs.___________________________________

___________

4

Parkman

Spring_______________________________________________

9

Brown's

Spring_________-_-____________________________________

10

Thundering

Spring___________________________________________

10

Barker

Spring.._______________________________________________

10

Lifsey

Spring._________________________________________________

10

Taylor

Spring.________________________________________________

11

Summary

of

the

warm

springs_________--_-___-_______--__-_---_-

11

Cold

springs

of

the

region._-_-____--______________-----_---__-____-

11

Cold

Spring______________._____._________________ ._________

11

Trammel's

Spring.____________

________________________________

13

Blue

Spring___.__.__________________________________

13

Cold

chalybeate

springs._______________________________________

13

Summary

of

the

cold

springs.___________________________________

14

Chemical

character

of

the

waters.__-______________________--__--_-_-

15

Gases

in

the

spring

waters._________________________________________

21

Other

hydrologic

investigations____________________________________

21

Rainfall__________________________________________________

22

Water

levels

in

wells.__________________________________________

23

Streams

______________________________________________________

23

Rock

formations___-___---_-_.___-_________-_-__-____-__-____-_-_

25

Pre-Cambrian

rocks

north

of

Towaliga

fault

______________________

26

Carolina

gneiss____________________________________________

26

Snelson

granite_______---_______-_-_

v

---_____-_____-____--_

26

Pre-Cambrian

rocks

south

of

Towaliga

fault______________________

27

Sparks

schist_____________________________________________

27

Hollis

quartzite.__________

_______________________________

27

Manchester

schist________--______-______------_--------__-

29

Woodland

gneiss_______________-___--____--__-_-_---_-_-__

29

Cunningham

granite.______________________________________

30

Triassic

igneous

rocks.-_-_-_-_-_________-_-___-__--_-_-_--_---_

30

Tertiary

(?)

and

later

sedimentary

rocks_________-___-____-_-__-

30

Structural

features_________________________________________________

31

Source

of

the

Warm

Springs

water_________________________________

32

Source

of

the

heat

of

Warm

Springs

water.__________--__-__----_--__-

34

Source

of

the

Cold

Spring

water___________________________________

35

Measures

for

improving

the

Warm

Springs

___________________________

36

Index._________________________________________________________

39

in

ILLUSTKATIONS

PLATE

1.

Geologic

map

of

Warm

Springs

quadrangle,

Ga_-__

____

In

pocket

2.

Generalized

geologic

map

of

west-central

Georgia

and

east-

central

Alabama,

showing

location

of

Warm

Springs

quad-

rangle

and

principal

springs.

_____________________________

4

3.

Map

of

the

Warm

Springs

area

showing

sources

of

warm

water,

pools,

drains,

and

improvements.________

______________

4

4.

Relation

of

discharge

of

Warm

Springs

to

rainfall

and

ground-

water

level

at

Roosevelt

farm,

January

1,

1934,

to

June

30,

1935________________________________

12

5.

Weekly

average

discharge

of

North

Spring

and

weekly

rainfall

at

Roosevelt

farm_____

____________________________________

12

6.

Fluctuations

of

ground-water

level

in

four

wells

and

relation

to

rainfall,

eastern

part

of

Pine

Mountain

area_

____.___.__.___

20

7.

Outline

map

of

Pine

Mountain

drainage

basins

showing

stream

discharge

March

12,13,14,

23,1934_

_______________

24

8.

Outline

map

of

Pine

Mountain

drainage

basins

showing

average

stream

discharge

July

1,1934,

to

June

30,1935_

________

24

FIGUBE

1.

Cross

section

through

Pine

Mountain

and

Warm

Springs

showing

geologic

structure

and

probable

course

of

the

water

discharged

at

Warm

Springs_______._____-____--_____-_______-_-._

33

IV

THE

WARM

SPRINGS

OF

GEORGIA

THEIR

GEOLOGIC

RELATIONS

AND

ORIGIN A

SUMMARY

REPORT

By

D.

F.

HEWETT

and

G.

W.

CBICKMAY

ABSTRACT

Seven

groups

of

warm

springs

are

known

in

Georgia,

but

popular

interest

centers

in

Warm

Springs,

in

the

western

central

part

of

the

State,

which

is

improved

for

use

in

the

Georgia

Warm

Springs

Foundation.

A

geologic

study

shows

that

the

several

warm

springs

are

confined

to

a

belt

of

pre-Cambrian

metamorphic

rocks

and

that

their

general

distribution

is

determined

by

one

of

the

members,

the

Hollis

quartzite.

,A

hydrologic

study

that

extended

over

about

21

months

included

observations

on

rainfall,

water

levels

in

wells,

spring

and

stream

dis-

charge

from

an

area

of

32

square

miles,

and

chemical

character

and

temperature

of

the

water. The

data

show

that

the

water

of

Warm

Springs

is

that

which

falls

on

the

crest

of

Pine

Mountain

and

is

carried

in

the

Hollis

quartzite

to

a

depth

of

about

3,000

feet

so

that

it

absorbs

heat

from

the

rocks

and

is

delivered

at

the

surface

with

a

temperature

of

88°

F.

INTRODUCTION

Long

before

the

War

between

the

States, Warm

Springs,

Ga.,

was

a

health

and

bathing

resort

for

the

people

of

the

region.

In

recent

years,

and

especially

since

the

establishment

in

1926

of

the

Georgia

Warm

Springs

Foundation

for

the

treatment

of

victims

of

infantile

paralysis,

with

the

improvement

of

the

springs

and

the

erection

of

adequate

buildings,

interest

in

the

area

has

greatly

broadened.

The

group

of

springs,

some

of

them

warm,

along

the

north

base

of

Pine

Mountain

have

long

been

recognized

as

presenting

interesting

geologic

problems

worthy

of

study.

Why

are

these

springs

found

where

they

are?

Why

are

some

warm

and

others

cold?

What

is

the

source

of

the

warm

water?

Is

all

or

a

part

of

it

derived

from

great

depths,

possibly

from

the

same

sources

as

igneous

rocks,

or

is

all

or

a

part

of

it

water

that

has

fallen

as

rain

on

the

surface?

By

what

channels

does

it

rise

to

the

point

of

outlet?

What

improvements

might

be

made

to

conserve

the

warm

water

and

to

maintain

or

increase

its

temperature?

These

are

questions

that

require

geologic

research

for

their

solution.

Funds

allotted by

the

Public

Works

Administration

in

1933

enabled

the

Geological

Survey

to

undertake

a

study

of

these

problems.

I

2

THE

WARM

SPRINGS

OF GEORGIA

SCOPE

OF

THE

INVESTIGATION

The

program

included

a

geologic

reconnaissance

of

a

large

part

of

the

region,

the

making

of

a

geologic

map

of

the

Warm

Springs

quad-

rangle

(pi.

1)

for

which

a

new

topographic

base

map

was

prepared,

and

a

detailed

study

of

the

geologic

features

of

the

part

of

Pine

Mountain

that

lies

near

Warm

Springs.

Inits.&y

;

eb^logic^f*eote

the

investiga-

tion

included

a

study

of

the

distribution,

environment,

discharge,

chemical

character,

and

temperature

of

the

spring

waters-of

tkeregpsm;

also,

because

of

their

bearing

on

the

probable

source

of

the

spring

waters,

measurements

of

the

local

rainfall

and

of

water

levels

in

select-

ed

wells,

and

determinations

of

the

distribution

of

the

run-off

of

the

streams

from

an

area

of

32

square

miles

on

Pine

Mountain near

Warm

Springs.

Field

studies

in

the

region

extended

from

October

1,

1933,

to

June

30,

1935.

This

report

presents

in

brief

form

the

essential

data

and

outstanding

conclusions

of

each

phase

of

the

investigation.

Inasmuch

as

interest

centers

on

the

springs,

only

such

geologic

data

as

are

necessary

to

their

study

are

presented

here.

A

complete

report

is

in

preparation.

ACKNOWLEDGMENTS

In

a

full

sense,

this

was

a

cooperative

investigation.

The

Georgia

Department

of

Forestry

and

Geological

Development

cooperated

with

the

Geological

Survey,

of

the

United

States

Department

of

the

Interior,

in

the

broad

plan

and

in

the

study

of

the

geologic

features

of

the

region.

O.

E.

Meinzer,

W.

D.

Collins, L.

K.

Wenzel,

and

other

members

of

the

water-resources

branch

of

the

Federal

Survey

cooper-

ated

in the

planning

and

execution

of

the

field

and

laboratory

work.

W.

L.

Lamar,

also

of

the

Federal

Survey,

collected

numerous

samples

of

water

and

made

all

water

analyses.

Analyses

of

the

gases

were

made

by

W.

P.

Yant,

of

the

Bureau

of

Mines.

The

equipment

for

measuring

rainfall

and

stream

and

spring

discharge

was

installed

by

C.

E.

McCashin

and

D. H.

Barker,

resident

engineers

in

the

Mont-

gomery

office

of

the

Geological

Survey.

From

March

to

September

1934

L.

D.

Cannon,

of

the

Georgia

Warm

Springs

Foundation,

made

observations

on

rainfall,

water

levels

in

wells,

and

spring

discharge.

From

September

1934

to

June

30,

1935,

D.

E.

Booth,

engineer, was

employed

to

make

all

local

observations

and

measurements.

C.

E.

Van

Orstrand,

of

the

Geological

Survey,

gave advice

concerning

the

method

of

measuring

earth

temperatures

and

supplied

the equipment

used

for

that

purpose.

SURFACE

FEATURES

Most

of

the

Warm

Springs

quadrangle

is

a

gently

rolling

upland,

known

as

the

Greenville

Plateau,

above

which rise

two

persistent

ridges,

Pine

and

Oak

Mountains,

and

into

which

the

streams

have

WARM

SPRINGS

OF

THE

REGION

3

carved

small

open

valleys.

The

entire

area

lies

within

the

broad,

relatively flat

belt

of

central

Georgia

known

as

the

Central

Upland,

a

local

subdivision

of

the

Piedmont

province.

South

of

it

lies

the

lower,

flat

Coastal

Plain

region

that

makes

up

the

south

half

of

the

State,

and

to

the

north

lies

a

mountainous

region

that

comprises

parts

of

th©^Lookout

Plateau,

the

Valley

and

Ridge

province,

and

the

Appalachian

Highlands.

1

In

the

vicinity

of

Warm

Springs

the

rolling

upland

lies

at

an

altitude

of

760

to

980

feet.

Above

it

Pine

Mountain

rises

to

altitudes

that

range

generally

from

1,100

to

1,200

feet,

but

at

Dowdell

Knob

it

attains

the

maximum

of

1,395

feet.

In

this

region

Pine

Mountain

departs

from

the

simple

linear

ridge

that

is

characteristic

of

most

of

its

length

in

western

Georgia.

South

of

Warm

Springs

it

broadens

to

a

flat-topped

mountain

3

miles

wide,

and eastward

the

ridge

joins

a

peculiar

circular

ridge

that

encloses

the

depression

locally

known

as

the

Cove.

Near

the

southern

border

of

the

Warm

Springs

quad-

rangle

is

Oak

Mountain,

a

linear

ridge

that

largely

ranges in

altitude

from

900

to

1,100

feet

and

therefore

rises

several

hundred

feet

above

'the-adj&ee&t

plateau.

The

dominant

streams

of

west-central

Georgia

are

the

Flint

and

Chattahoochee

Rivers,

both

of

which

flow

generally

southward.

The

Flint

River

lies

within

the

eastern border

of

the

Warm

Springs

quadrangle,

and

many

of

the

minor

streams

of

this

region

drain

east-

ward

and

southeastward

to

it.

The

Chattahoochee

River

lies

beyond

the

western

border

of

the

quadrangle,

and

several

streams

of

this

region

flow

westward

and

southwestward

to

it.

The

divide

between

the

streams

that

are

tributary

to

these

two

rivers

extends

northward

from

Warm

Springs.

In

its

primitive

state,

all

of

this

region

was

doubtless

covered

with

dense

forest,

mostly

oak

and

other

hardwoods

but

including

pine

of

/-several.

varieties.

At

present

about

two-thirds

of

the

-area

north

of

Pine

Mountain

has

been

cleared

and

is

under

cultivation. About

half

of

the

area

south

of

Pine

Mountain

has

been

cleared.

On

Pine

Mountain

the

lower

slopes

are

locally

cleared

and in

part

are

planted

with

orchards.

Most

of

the

marketable

timber

has

been

removed

from

the

forest areas

by

selective

cutting.

Although

the

rocks

under-

lying

the

upland

of

the

Greenville

Plateau

are

of

different

kinds,

the

residual

soils

have*

much

resemblance,

and

all

are susceptible

to

erosion

and

gullying,

with

the

result

that

large

areas

have

been

ren-

dered

unfit

for

further

cultivation.

WARM

SPRINGS

OF

THE

REGION

The,

known

«Wlfem;

springs

of

Georgia

are

found

in

a

belt

that

ex-

tends

from

Barnesville

southwestward

about

40

miles

to

Warm

Springs.

It

has

been

known

for

more

than

a

hundred

years

that

the

i

LaForge,

Laurence,

Physical

geography

of

Georgia: Oeorgia

Oeol.

Survey

Bull.

42,

pp.

77-80,

1925.

4

THE

WABM

SPRINGS

OP

GEORGIA

waters

of

some

of

these

springs

were

appreciably

warm,

and

when

the

present

investigation

was

undertaken

the

pools

produced

by

five

of

the

springs Warm

Springs,

Thundering

Spring,

Barker

Spring,

Lifsey

Spring,

and

Taylor

Spring

(pi.

2) had

been

used

from

time

to

time

for

either

swimming

or

bathing.

During

this

investigation

two

more

warm

springs

were

discovered,

Parkman

and

Brown's

Springs,

and

additional

sources

of

warm

water

were'

found

near

Thundering

Spring.

The

spring

having

the

highest

temperature,

Warm

Springs

(88°

F.),

has

also

the

largest

discharge

(594

to

678

gallons

a

minute), and

the

warm

spring

having

the

lowest

temperature,

Brown's

Spring

(69°

F.),

has

the

smallest

discharge

(15

to

30

gallons

a

minute).

According

to

the

records

of

the

United

States

Weather

Bureau,

the

average

air

temperature

at

West

Point,

28

miles

west

of

Warm

Springs,

is

63.3°

F.,

and

at

Talbotton,

17

miles

southeast,

64.1°

F.

The

aver-

age

temperature

of

the

water

in

36

wells

in

the

lowland

adjacent

to

the

Pine

Mountain

area

is

62.1°

F.

In

this

investigation

springs

whose

temperature

is

higher

than

66°

F.

have

been

classified

as

warm.

All

these

warm

springs,

as

well

as

several

large

cold

springs,

issue

in

the

Wacoochee

belt,

a

large

part

of

which

is

made

up

of

a

series

of

altered

sedimentary

rocks,

called

by

Galpin

3

the

Pine

Mountain

formation

(pi.

2).

This

series

extends

from

Barnesville

southwest-

ward

almost

to Notasulga,

Ala.,

a

distance

of

100

miles.

The

most

conspicuous

unit

of

the

series

is

a

formation

known

as

the

Hollis

quartzite,

usually

275

to

800

feet

thick

in

this

region.

In

the

part

of

the

belt

under

consideration

the

quartzite

underlies

a

group

of

extensive

but

poorly

defined

ridges

that

make

up

Pine

Mountain,

which

here

rises

200

to

500

feet

above

the

surrounding

upland.

All

the

warm

springs

issue

at

the

surface

in

the

upland

areas,

near

the

ridges.

All

except

Warm

Springs

rise

through

the

Manchester

schist,

which

overlies

the

quartzite,

or

through

local

alluvium.

Warm

Springs

(no.

1,

pi.

2). The

warm

springs

for

which

this

region

has

become

nationally

famous

issue

at

the

north

base

of

a

low

knoll

which

is

the

site

of

the

Georgia

Warm

Springs

Foundation.

They

are

half

a

mile

west

of

the

town

of

Warm

Springs,

where

the

Columbus

branch

of

the

Southern

Kailway

crosses

the

Atlanta,

Birmingham

&

Coast

Kailway,

which

extends

from

Brunswick,

Ga.,

to

Birmingham,

Ala.

The

population

of

the

town

of

Warm

Springs

is

about

300,

but

250

more

reside

at

the

Foundation. The

pools

and

bathhouses

used

for

therapeutic

treatments

are

adjacent

to

the

springs

(pi.

3),

but

the

other

buildings

x

of

the

institution

are

in

fc

grove

of

pine

and

oak

that

covers

the

knoll.

About

200

acres

of

land

that

includes

the

knoll

and

the

springs

is

owned

by

the

Georgia

Warm

Springs

Foundation,

an

incorporated

nonprofit

organization.

This

investigation

reveals

a

record

of

the

springs

as

early

as

1819,

when

they

were

improved

with

bathhouses

and

there

was

a

1

Galpin,

S.

L.,

Feldspar

and

mica deposits

of

Georgia:

Georgia

Geol.

Surrey

Boll.

30,

p.

74,1915.

GEOLOGICAL

SUBVEY

WATER-SUPPLY

PAPER

819

PLATE

3

84°

ndian

Springs

o

%,

O

THOMASTON

LIST

OF

SPRINGS

1.'Warm

Springs

6.Lifsey

Sprin

2.

Parkman

Spring

7.

Taylor

Sprin

3.

Brown's

Spring

8-Blue

Spring

4.

Thundering

Spring

9.

Trammels

Spring

5.

Barker

Spring

EXPLANATION

Chewacla

marble

Known

outcrop

of

Hollis

quartzite

GENERALIZED

GEOLOGIC

MAP

OF

WEST-CENTRAL

GEORGIA

AND

EAST-CENTRAL

ALABAMA,

SHOWING

LOCATION

OF

WARM

SPRINGS

QUADRANGLE (SHADED

AREA)

AND

PRINCIPAL

SPRINGS

(NUMBERED).

GEOLOGICAL

SURVEY

WATER-SUPPLY

PAPER

819

PLATS

3

EXPLANATION

«43

Point

of

measurement

of

discharge

and

temperature

Numbers

correspond

to

those

in

table

in

text

MAP

OF

THE

WARM

SPRINGS

AREA,

SHOWING

SOURCES

OF

WARM

WATER,

POOLS,

DRAINS,

AND

IMPROVEMENTS

Numbers

indicate

points

where

discharge

was

measured.

WARM

SPRINGS

OF

THE

REGION

$

liotel

nearby,

but

doubtless

they

were

in

use

long

before

that

time.

8

In

187

5

the

water

was

conveyed

by

an

open

ditch

to

six

uncovered

masonry

chambers,

each

10

by

10

feet, which

were

used

for

bathing.

These

masonry

chambers,

now

covered

with

concrete

roofs,

are

used

as

a

reservoir

from

which

the

water

is

distributed

to

the

places

of

use.

Plate

3

shows

the

known

sources

of

warm

water

and

the

build-

ings

that

have

been

erected

to

use

it.

The

main

sources

of

warm

water

lie

south

of

the

group

of

masonry

chambers,

but

minor

sources

are

found

as

much

as

250

feet

to

the

east

and

250

feet

to

the

west.

At

present

only

the

water

from

the

main

sources

is

under

control for

use.

From

December

14,

1933,

to

June

30, 1935,

the

discharge

under

control

ranged

from

594

to

678

gallons

a

minute

(pp.

7-9).

Measurements

of

,the

discharge

of

all

the

minor

sources

during

the

same

period

ranged

from

233

to

294

gallons

a

minute

(p. 9).

The

total

discharge

of

all

sources,

therefore,

ranged

from

844

to

914

gallons

a

minute.

Several

measurements

made

as

much

as

40

years

ago

indicated

a

discharge

of

666

to

1,890

gallons

a

minute,

but

when

the

place

and method

of

measurement

are

considered,

there

is

no

reason

for

thinking

that

the

total

discharge

from

all

sources

has

varied

greatly-^-probably

not

more

than

20

percent during

this

period.

The

main

source

of

the

supply

may

be

examined

in

a chamber

24

feet

long

and

4

feet

high

that

lies

south

of

the

eastern

group

of

three

masonry

chambers

(pi.

3).

Most

of

this

chamber

is

lined

with

loosely

laid

quartzite

blocks,

from

the

cracks

of

which

considerable

water

issues,

but

a

recess

in

the

wall

reveals

an

open

fissure

in

hard

quartzite

from

which

about

200

gallons

a

minute

is

flowing

almost

horizontally.

Some

water and

bubbles

of

gas

rise

from

the

sand

that

covers

the

bottom

of

the

eastern

two

chambers.

The

only

additional

water

that

enters

the

reservoir about

75

gallons

a

minute is

discharged

from

a

hole

in

the south

wall

of

the

westernmost

of

the

six

chambers,

but

the

conditions

behind

the

wall

are

not

known.

Precise

measurements

of

the

temperature

of

the

Warm

Springs

water

as

it

issues

from

the

ground

at

its

main

east and

west

sources

were

made

on

seven

different

days

in

1933,1934,

and

1935

by

using

a

platinum

resistance thermometer.

At

the

east

source

the

temperature

on

different

days

ranged

from

87.7°

to

88.2°

F., and

at

the

west

source

from

87.1°

to

87.5°

F.

On

the

same

day

the

temperature

at

the

east

source

was

found

to

be

0.6°

to

0.7°

F.

higher

than

the

west

source.

A

recording

thermometer

reading

to

single

degrees

was

*

White,

George,

Statistics

of

Georgia,

p.

424,1849;

Historical

collections

of

Georgia,

p.

550,1854.

Walton,

G.

E.,

Mineral

springs

of

the

United

States

and

Canada,

p.

810,1878.

Duggan,

J.

R.,

Mineral

springs

of

Georgia,

p.

53,1881.

Weed,

W.

H.,

Notes

on

certain

hot

springs

of

the

southern

United

States:

Geol.

Survey

Water-Supply

Paper

145,

pp.

187-189,

1905.

Hall,

B.

M.

and

M.

R.,

Water

resources

of

Georgia:

Geol.

Survey

Water-Supply

Paper

197,

p.

14,1907.

McCallie,

S.

W.,

Mineral

springs

of

Georgia,

p.

166,

Georgia

Geol.

Surrey,

1913.

Watson,

T.

L.,

Thermal

springs

of

the

southeast

Atlantic

States;

Jour,

Geology,

vol.

82,

pp.

380-382,1924.

,

15468 37

2

6

THE

WARM

SPRINGS

OF

installed

in

the east

source

in

April

1934,

and

during

the

following

year

and

a

half

it

indicated

that

the

temperature

at

this

source

varied

less

than

1°

F.

The

locations

of

the

places

where

the

discharge

from

minor

sources

was

measured

are

shown

on

plate

3.

Doubtless

there

are

other

sources

in

this

area,

but

they

cannot

be

identified

now.

Stated

broadly,

warm

water

issues

from

numerous

sources

in

a

narrow

belt

about

500

feet

long

that

closely

follows

the

base

of

a

hill

of

quartzite

where

it

meets

a

local

plain

underlain

by

unconsolidated

alluvium.

Most

of

the

water,

about

550

gallons

a

minute,

is

discharged

from

the

middle

25

feet

of

this

belt,

and this

water

shows

the

highest

temperature.

During

the

investigation

the

temperature

of

this

water

ranged

from

87.6°

to

88.2°

F.

Progressively

outward,

both

east and

west,

from

this

middle

part,

the

discharge

of

the

separate

sources

was

lower

and

the

temperature

of

the

water

was

lower,

dropping

to

83°

F.

at

the

westernmost

source

and

to

79°

F.

at

the

easternmost

source.

In

order

to

understand

some

of

the

influences

that

affect

the

dis-

charge

of

Warm

Springs,

an

attempt

was

made

to

measure

it

every

day.

As

the

present

facilities

for

using

the

water

represent

the

suc-

cessive

additions

to

those

installed

many

years

ago

and

as

the

drafts

upon

the

discharge

are continuous,

measurement

proved

difficult.

After

careful

examination,

the

conclusion

was

reached

that

the

dis-

charge

could

be

measured

best

by

diverting

all

the

water

from

the

covered

reservoir

to

the

public

pool

and

measuring

accurately

the

time

required

to

raise

the

water

level

in

the

pool

a

definite

amount,

usually

0.8

foot.

The

beginning

and

end

of

each

measurement

were

determined

by

using

a

hook

gage

placed

in

a

stilling

well

at

the

north-

east

corner

of

the

pool

(pi.

3).

The

area

of

the

pool

was

determined

to

be

10,490

square

feet;

therefore

the

volume

of

water

usually

measured

was

8,392

cubic

feet,

or

62,776

gallons.

The

duration

of

the

tests

ranged

from

95

to

105

minutes,

but

it

was

necessary

to

control

con-

ditions

around

the

spring

for

nearly

3

hours

every

day.

At

least

two

influences

are

known

to

affect

the

rate

of

discharge

of

springs the

pressure

head,

under

which

the

water

appears

at

the

surface,

and the

atmospheric

pressure,

which

tends

to

resist

and

offset

the

pressure

head.

Early

in

the

investigation

it

was

shown

by

experi-

ment

that

the

water

of

Warm

Springs

rises

under

considerable

pressure.

To

determine

the

fluctuations

in

atmospheric

pressure,

a

recording

barograph

was

installed

and

maintained

from

October

1,

1934,

to

June

30,

1935.

Careful

comparison

of

this

barometric

record

with

that

of

the

spring

discharge

shows

that

changes

in

atmospheric

pressure

have

only

slight

effect

on

the

discharge,

thus

indicating

that

there

is

considerable

head

at

the

outlet.

The

following

table

gives

the

measurements

of

discharge

made

during

this

investigation.

1

SPRINGS

OF

THE

REGION

Flute

4

presents

the

graph

of

discharge

calculated

as

the

running

average

over

2

weeks

for

each

week

covered

by

the

investigation.

The

record

was

intermittent

through

the

spring

of

1934

but

was

regular

and

very

reliable

from

August

1,

1934,

to

June

30,

1935.

Measurements

of

discharge

of

Warm

Springs,

in

gallons

a

minute

Date

1933

Tlfln

14

Dec

15

Dec.

19..........

Dec

20

r»n«

9Q

nn«

in

1934

Jan.

11

Jan.

12

...

.

Jan.

17

...

Jan.

19

Jan.

22...-.. ..

Jan.

23

....

Feb.

9.

_

.

Mar.

15..

__

--

Mar.

16

Mar.

22 .

Mar,26

Mar.

27

.

Mar.

28

.

Mar.

30

.

Apr.

9

...............

Apr.

21..

_

.........

May

1-.

____

--..

May

16

____

..

May

17..

....

May

23.

...

-

July. .. ..

Aug.

6...

...

Aug.

8

-_-._

Aug.

10..

.....

.

Aug.

11..

.......

...

-.

Aug.

13-

...

Aug.

14..

...

--..

Aug.

15

-

Aug.

16..

...

-

Aug.

18..

......

...

Aug.

20.....

......

Aug.

21.

..!....

......

Aug.

22.

.............

Aug.

23.

...

....

.

Aug.

24

..............

Aug.

25..

...

.

Augr2T...

__

.......

Aug.

28.

.....

Aug.

29..

.

Aug.

30..-

...

..

Sept.

1...

.-

_

-.--

...

Sept.

4... ..

Daily

rate

623.7

626.

9

615.7

630.7

621. 4

614.8

620.2

636.2

618.4

623.6

628.7

615.7

fl91

9

628.7

618.8

621.6

614.8

615.7

617.2

618.4

631.8

619.4

613.6

619.9

COO

A

637.5

636.7

622.1

619.7

634.5

fiQO

A

622.4

620.4

632.4

623.6

633.4

639.

5

642.7

629.0

632.4

0)

650.5

662.6

642.7

645

0

651.8

649.1

663.3

652.8

644.6

667.2

651.0

670.4

651.0

678.6

656.6

653:2

630.1

663.0

653.2

632.4

636.7

Average

for

week

622.1

626.0

622.4

619

9

623.1

619.4

613.6

621.4

620.9

637.1

632.4

652.0

650.8

656.8

655.9

Running

average,

2

weeks

623.7

fi91

Q

fi9l

Q

623.1

619.4

613.6

fi9Q

Q

629.7

fi97

9

635.9

651.29

653.8

656.2

648.9

Date

1934

Sept.

5

Sept.

7...

...

.

Sept.

8

Sept.

11.

Sept.

12..

_____

..

Sept.

14.

_

...

.-

Spnt

1

Q

Sept.

20

_

.

_

.

Sept.

21

Sept.

24

Sept.

25.

____

-..-

Sept.

27.

Sept.

28...

_

.

__

-.

Sept.

29

Oct.

I....'

Oct.

2....

...........

Oct.

5....

....

...

.

Oct.

6....

Oct.

8...

Oct.

9

...

Oct.

10.......

.-

Get:

11.

___

.

..

.

Oct.

12..,

Oct.

13... -

Oct.

15

Oct.

16..

_____

..--

Oct.

17

Oct.

18......

Oct.

19

__

.

___

--

Oct.

20

__

-

__

..--

Oct.

22... . -

Oct.

23

Oct.

24

_

.

___

.....

Oct.

25...

Oct.

26...

Oct.

27

Oct.

29......

.....

....

Oct.

30

_

.

_____

..

Oct.

31......

.......

-

Nov.

1_

....

.

Nov.

2.

......

.

Nov.

3.

...

Nov.

8.

........

Nov.

13..

Nov.

16

Nov.

17.

Nov.

20..

....

Nov.

21.

Nov.

23..

Nov.

24....

Nov.

27.

Nov.

28.

Nov.

29

Dec.

3.....

..-

Dec.

5...

....

Daily

rate

636.7

606.7

607.2

602.3

621.4

627.8

617.5

599.0

621.6

615.7

623.1

618.8

631.8

622.0

620.2

619.2

614.8

611.2

612.6

619.3

610.3

606.3

609.0

614.4

607.2

606.3

612.6

607.2

612.2

614,0

612.2

613.6

606.3

609.5

908.1

609.9

607.2

608.6

605.9

605.3

fins

i

607.2

606.3

fiOA

3

600

1

604.5

605.3

609 9

604.5

602.3

606.3

614.8

611.7

612.6

619.0

628.7

616.3

620.2

606.0

618.1

612.2

618.0

615.6

610.8

617.1

618.0

612.2

Average

for

week

635.3

613.1

613.4

623.2

614.4

611.1

610.7

fido

Q

607.0

605.6

607.9

618.4

614.0

Running

average,

2

weeks

621.4

613.2

618.3

618.8

612.7

610.9

610.3

608.5

606.2

606.5

613.6

616.4

613.9

1

No

measurements;

leaks

in

main

pipe

stopped.

8

THE

WARM

SPRINGS

OF

GEORGIA

Measurements

of

discharge

of

Warm

Springy

in

gallons

a

minute

Continued

Date

1934

Dec.

6..

.............

Dec.

8.

_______

Dec.

10

..............

Dec.

11.

_____

...

Dec.

12.

_

..

__

...

Dec.

13...

_

.

___

Dec.

14.

_

.....

_

..

Dec.

IS.......

.......

Dec.

16

______

.

Dec.

17

..............

Dec.

18...

__

....

...

Dec.

19...

__

.......

Dec.

20

__

.

.........

Dec.

21

..............

Dec.

22........

__

.

Dec.

23.....

_

......

Dec.

24

______

.

Dec.

25

..............

Dec.

26...

_

........

Dec.

27

_____

....

Dec.

28...

_____

.

Dec.

29.

___

......

Dec.

30.

_______

Dec.

31..

_____

.

1935

Jan.

1................

Jan.

2.

...............

Jan.

3

__

. .

Jan.

4

__

.

_

.....

Jan.

5

................

Jan.

6

_

.

Jan.

7

............

Jan.

8

................

Jan.

9

___

.

.......

Jan.

10

_____

..

Jan.

11

__

....

.....

Jan.

12...............

Jan.

13...............

Jan.

14

_

...

Jan.

15

__

..

....

Jan.

16.

......

Jan.

17

...........

Jan.

18

...............

Jan.

19.

...........

Jan.

21.

_____

..

.

Jan.

22

_

...........

Jan.

23

_______

.

Jan.

24.

_

...........

Jan.

25..

.....

Jan.

26

.............

Jan.

27

...............

Jan.

28...............

Jan.

29...............

Jan.

30.... .....

Jan.

31

...............

Feb.

1.

..............

Feb.

2.

_

.

_

.......

Feb.

3.

.......

...

....

Feb.

5.. ...

Feb.

6

___

.........

Feb.

7..

.............

Feb.

8..

.............

Feb.

9...............

Feb.

10..

............

Feb.

11..........

....

Feb.

12

__

..........

Feb.

13...

__

......

Feb.

14.......

....

Feb.

15...

...

.

Feb.

16..

............

Feb.

17...... .....

Feb.

18-

...

......

Feb.

19..............

Feb.

20..

............

Feb.

21..............

Feb.

22........

__

.

Feb.

23.

__

..

_

....

Feb.

24..

............

Daily

rate

606.7

609.0

610.8

607.2

603.2

602.3

601.4

603.6

602.3

601.9

613.6

608.5

602.8

600.9

60S.

4

598.7

597.3

599.2

599.7

601.4

600.0

603.6

604.5

603.2

602.8

601.4

603.2

600.9

602.3

606.0

604.5

607.7

615.7

606.0

618.9

604.0

602.3

604.9

609.5

611.2

614.0

606.4

613.4

607.7

611.7

600.1

604.5

605.4

611.2

609.0

606.0

607.2

604.9

610.0

606.0

600.5

612.6

600.0

597.3

601.4

612.6

598.2

615.7

611.7

607.2

600.9

619.9

605.4

595.5

604.9

616.7

613.9

611.2

605.4

607.2

600.0

Average

for

week

613.9

605.8

fifU

B

600.2

CAO

0

608.7

608.1

607.3

607.8

604 4

606.8

609.6

Running

average,

2

weeks

609.8

605.3

602.5

601.5

605.8

608.4

607.8

607.6

(VIA

^

605.7

AnQ

O

AAQ

9

Date

1935

Feb.

25.

__

....

__

.

Feb.

26.

__

.........

Feb.

27

__

...

__

..

Feb.

28

__

..........

TV/Tan

1

TV/Tar

9

TWai-

9

TV/Tar

19

Mar.

14........

......

IVtar

19

IVtar

21

IV/Tar

OO

Mar.

23.

............

IVIsr

27

IVtar

29

TV/Tar

Qft

Apr.

1

____

.......

Apr.

2.......

.'.......

Apr.

4..

...

ATM*

H

A

rvr

ft

Apr.

10.

_

...

_

....

Apr.

11..........

....

Apr.

12..... . .-

Apr.

13.....

.

..

Apr.

15.......

.......

Apr.

16....

_

.....

Apr.

17.

__

....

Apr.

20-.. ..

Apr.

22...

__

.......

Apr.

23.

_

.

_

-

_

.

Apr.

24...

__

Apr.26

....

.

Apr.

27..

__

.

_

.

1WQT7

Q

TVTATT

1^

TVfo-tr

1

A

May

15.....

.....

May

16.

__

May

17.

____

....

.

TVT*nr

Ifi

TX^ftTr

9*>

May

23

__

.....

__

May2A.

__

May

27

_

... ...

May

28

___

.......

May

30

____

.......

May

31

__

...

....

DaUy

rate

616.2

610.8

607.2

594.2

firu

n

609.7

627.4

R1Q

Q

619.5

624.7

625.2

ftlQ

Q

617.2

611.7

619.5

625.6

627.0

632.4

632.8

625.6

630.1

R1Q

O

624.7

626.5

R1Q

O

617.1

626.0

626.9

632.4

628.7

626.9

653.4

640.0

630.1

629.7

626.5

622.4

620.7

622.5

625.1

624.6

625.6

627.8

630.2

632.6

635.2

638.8

635.2

625.6

619.7

626:.

9

626.6

629.4

631.8

610.0

614.0

R1Q

O

631.4

629.3

635.7

625.6

AK1

1

fsAn

«

633.5

621.6

Average

for

week

622.5

619.4

AOA

1

620.7

622.0

627.3

635.9

624.1

625.5

635.5

Running

average,

2

weeks

607.7

620.2

Aon

o

622.5

623.4

621.4

624.4

629.4

627.6

628.2

630.5

628.0

WABM

SPRINGS

OF

THE

REGION

9

Measurement

of

discharge

of

Warm

Springs,

in

gallons

a

minute

Continued

Date

1935

June

1

...............

June

10

..............

Daily

rate

616.6

616.2

618.4

614.8

612.6

616.6

609.5

612.6

609.0

610.8

Average

for

week

617.7

612.0

Running

average,

2

weeks

614.8

610.5

Date

1935

June

22

_

.

..........

June

28. .

......

Daily

rate

609.0

610.3

604.1

608.1

606.3

607.7

606.3

603.2

614.0

Average

for

week

608.5

606.8

608.6

Running

average,

2

weeks

608.0

607.4

Measurements

of

discharge

of

Warm

Springs

and

surface

drains

No.

on

plate

3

32

1..__....._....

...........

38

1

.......................

34

».

35....

___

....................

36 ...

__

....................

37 ..

__

..

38.

__

..

39

__

...

.......

..... .....

40

41

__

..

____

...

-

_____

..

42

______

.

_

.

____

.

Total

(no.

42

minus

no.

35).-

43.

....................

44

. . . .

45.

______________

....

46.

_____________

.

......

47

48

__

-...

49

__

._ _ .

50 .

Total

(no.

50

minus

no.

43)

~

Total

discharge

of

warm

water,

not

including

Warm

61

»

___

....

...........

Tem-

pera-

ture

Oct.

17-21,

1934

(°F.)

65

82

84

86

79

86

80

62

83

73

79

85

87

46

81

85

Discharge

(gallons

a

minute)

1934

Oct.

17-21

12.1

6.3

24.2

14.4

34.6

39.9

13.5

4.5

31.4

20.2

85.8

71.4

32.8

24.2

85.8

3.1

1.1

54.8

1.1

194.4

161.6

233.0

Nov.

18

10.8

76.8

66.0

1.7

194.0

192.3

258.3

Dec.

8

12.1

6.3

26.5

16.6

88.0

71.4

16.6

227.0

210.4

281.8

1935

Jan.

5-6

18.8

8.1

26.9

16.6

90.2

73.6

30.1

244.0

213.9

287.5

Jan.

26,27

20.2

7.2

20.2

14.4

83.5

69.1

2.2

220.0

217.8

286.9

Feb.

9

15.7

7.2

11.3

15.7

83.5

67.8

Feb.

23

22.0

5.8

18.8

15.7

89.9

74.2

15.7

235.0

219.3

293.5

Mar.

23

62.9

9.9

33.2

14.4

81.7

67.3

0

221.0

288.3

35

Apr.

30

49.8

12.1

37.3

14.4

85.8

71.4

0

184.0

255.4

May

30

9.0

3.1

28.3

14.4

69.1

54.7

13.5

210.0

196.5

251.2

i Minor

cold

streams

east

of

area

shown

on

plate

3.

'

Spring

51

could

be

measured

only

when

the

water

of

the

pond

was

drained.

Parkman

Spring

(no.

2,

pi.

2). Parkman

Spring

was

identified

in

December

1933,

within

the

present

area

of

Parkman's

pond

at

a

time

when

it

was

drained

to

a

low

level.

The

pond

is

created

by

a

dam

below

the

junction

of

two

broad

valleys

that

drain

the

eastern

slope

of

a

spur

from

Pine

Mountain.

The

discharge

was

estimated

to

be

between

50

and

100

gallons

a

minute,

and

the

temperature

of

the

main

source

on

December

10,

1933,

was

76.6°

F.

An

analysis

of

the

water

appears

in

the

table

on

page

17.

10

THE

WARM

SPRINGS

OF

GEORGIA

Brown's

Spring

(no.

3,

pi.

2). Brown's

Spring

is

about

4

miles

northeast

of

Manchester,

in

the

low

ground

south

of

the

ridge

that

encloses

the

Cove.

Three

distinct

sources

of

water

appear

within

an

area

about

100

feet

in

diameter,

but

most

of

the

water

issues

from

the

southwest

source,

a

pool

about

5

feet

across.

A

little

gas

issues

from

this

pool.

Quarterly

measurements

from

December

1933

to

Decem-

ber

1934

indicate

that

the

discharge

ranges

from

15

to

30

gallons

a

minute.

The

temperature

of

the

main

source

was

69.0°

F.

on

Decem-

ber

8,

1933,

68.4°

F.

on

March

24,

1934,

and

68.1°

F.

on

June

14,

1935.

Two

analyses

appear

in

the

table

on

page

17.

Thundering

Spring

(no.

4,

pi.

2). Thundering

Spring

is

about

5

miles

southeast

of

Woodbury.

The

main

spring

rises

in

low

swampy

ground

on

the

north

slope

of

a ridge

and

was

once

surrounded

by

a

frame

enclosure,

so

that

the

pool

could

be

used

for

bathing.

The

principal

source

now

lies

in

the

center

of

a

dirty

pool

that

is

fed

by

a

surface

stream and

is

indicated

by

a vigorous

discharge

of

gas

bubbles,

from

which

the

name

was

derived.

During

the

investigation

the

water

of

the

surface

stream

proved

to

be

warmer

than

the

normal

for

the

region

and

to

contain

more

bicarbon-

ate

than

surface

water

generally.

This

led

to

the

discovery

of

four

other

sources

of

warm

water

in

a

triangular

area

1,000

feet

south

of

the

main

spring.

The

total

discharge

from

all

these

sources

in

June

1935

was

380

gallons

a

minute.

The

temperature

of

the

main

spring

was

74.2°

F.

on

March

23,

1934,

and

73.9°

F.

on

June

12,

1935.

Two

analyses

are

shown

in

the

table

on

page

17.

Barker

Spring

(no.

5,

pi.

2). Barker

Spring

is

south

of

State

High-

way

74,10

miles

southeast

of

Molena.

It

originally

issued

in

alluvium

in

the

low

ground

near

a

ridge

of

Hollis

quartzite,

but

it

is

now

en-

closed

by

concrete

walls

so

as

to

form

a

pool

28

by

98

feet,

which

is

used

for

swimming.

Numerous

sources

can

be

identified

by

the

gas

bub-

bles

that

rise

from

the

bottom.

In

November

1933

the

discharge

was

30

gallons

a

minute. The

temperature

in

the

largest

source was

73.4°

F.

on

March

23,

1934,

and

74.2°

F.

on

June

12,

1935.

Two

analyses

are

shown

in

the

table

on

page

17.

Li/sey

Spring

(no.

6,

pi.

2). Lifsey

Spring

issues

from

alluvium

in

low

ground

200

feet

north

of

a

county

road

that

extends

westward

2

miles

from

Pine

Mountain

Store,

4

miles

south

of

Zebulon.

Numerous

sources

of

water

are

enclosed

within

concrete

walls

so

as

to

form

a

pool

32

by

98

feet,

which

is

used

for

swimming.

Bubbles

of

gas

rise

spasmodically

from

the

largest

sources.

Measurements

in

June

1935

showed

a

total

discharge

of

83

gallons

a

minute.

The

temperature

on

June

15,

1935,

measured

by

placing

the

thermometer

bulb

on

the

bottom

of

the

pool

at

places

where

the

water

was

clear,

was

found

to

be

78.5°

F.

The

air

temperature

at

the

time

was

84°

F.,

and

the

temperature

of

the

water

at

the

surface

of

the

pool

was

78.8°

F.

An

analysis

of

the

water

appears

in

the table

on

page

17.

COLD

SPRINGS

OF

THE

REGION

H

Taylor

Spring

(no.

7,

pi.

2). Taylor

Spring

rises

in

the

alluvium

of

a

wide

valley

900

feet

west

of

U.

S.

Highway

19,

6.5

miles

south

of

Zebulon.

The

course

of

the

stream

that

drains

the

valley

has

been

diverted

to

a

new

channel,

and

the

sources

of

water

have

been

enclosed

by

an

earth

embankment

so

as

to

form

a

pool

350

feet

long

and

100

feet

wide

at

the

lowest

end.

From

this

reservoir

water

is

drawn

to

a

con-

crete

pool

40

by

130

feet,

which

is

used

for

swimming.

In

June

1935

the

spring

discharge

was

385

gallons

a

minute.

The

temperature

of

the

water

issuing

from

the

springs

hi

the

upper

part

of

the

reservoir

was

74.8°

F.

on

June

15,1935.

An

analysis

of

the

water

appears

in

the

table

on

page

17.

Summary

of

the

warm

springs.

Although

this

investigation

was

focused

on

the

features

and

environment

of

Warm

Springs,

it

seemed

desirable

to

make

general

and

intermittent

observations

of

all

the

other

warm

springs

that

were

known

or could

be

found

in the

region.

There

may

be

unrecorded

small

springs

of

warm

water

in this

general

region,

but

it

is

believed

that

all

that

exist

in

the

Warm

Springs

quadrangle

have

been

found.

The

temperature

and

chemical

char-

acter

of

the

warm

waters

were

surprisingly

constant

during

the

period

of

study.

The

discharge

of

Warm

Springs

varies,

but

not

as

much

as

that

of

the

cold

springs

of

the

region;

the

maximum

discharge

was

only

14

percent

more

than

the

minimum.

Conditions

were

not

favorable

for

making

numerous

precise

measurements

of

discharge

of

the

other

warm

springs.

The

chemical

character

of

the

warm

waters

is

dis-

tinctive.

(See

p.

15.)

The

geologic

relations

of

the

warm

springs

are

discussed

on

pages

32-35.

COLD

SPRINGS

OF

THE

REGION

At

many

places

in

this

region

there

are springs

that

discharge several

gallons

a

minute

of

clear

cool

water.

These

are

commonly

found

on

the

lower

slopes

of

hills

and

ridges.

Such

springs

are

abundant

in

most

regions

where

the annual

rainfall

is

40

inches

or

more.

At

a

few

places

in

this

region,

however,

there

are

springs

that

discharge

several

hundred

gallons

a

minute

or

more

of

cool

water,

and

interest

is

at-

tached

to

their

origin.

Among

the

springs

that

discharge

only

a

few

gallons

a

minute,

there

are

some

that

deposit

hydrated

oxide

of

iron.

Analyses

show

that

the

water

from

such

springs

contains

much

more

iron

than

other

waters,

and

they

are

commonly

known

as

chalybeate

springs.

Cold

Spring.

Within

an

area

of

about

8

acres

about

a

mile

south-

east

of

Warm

Springs,

there

are

four

distinct

springs

which,

for

the

purposes

of

this

investigation,

have

been

called

Cold Spring,

North

Spring,

and

South

Springs

nos.

1

and

2.

The

assemblage

is

locally

known

as

Cold

Spring.

All

are

found

within

a

reservation

used

as

a

fish

hatchery

by the

United

States

Government.

This

investiga-

tion

indicates

that

any

influence

which

affects

the

discharge

of

Cold

12

THE

WARM

SPRINGS

OF

GEORGIA

Spring

also

affects

that

of

North

Spring

and

that

they are

closely

related.

The

South

Springs,

which

are

about

30

feet

apart,

are

700

feet

southeast

of

North

Spring;

They

seem

to

be

separate

outlets

of

the

same

source

of

water

but

are

not

closely

Cold

and

North

Springs.

Each

of

the

four

springs

is

enclosed

in

a

wall

of

concrete

or

masonry.

The

water

of

Cold

Spring

is

used

for

several

purposes.

A

part

is

drawn

to

four

rams

800

feet

to the

northwest,

which

pump

a

part

of

the

water

to

an

elevated

tank

that

supplies

the

town

of

Warm

Springs.

A

part

is

drawn

to

two

other

rams

which

supply

nearby

private

houses.

Of

the

remainder,

a

part

is

drawn

to

a

small

reservoir

known

as

the

rock

house,

at

the

fish

hatchery.

The

water

from

North

Spring

supplies

the

pools

of

the

hatchery;

that

of

the

South

Springs

is

used

by

local

residents.

The

unused

and

waste

water

from

all

these

sources

constitutes

the

principal

supply

of

Cold

Spring

Branch.

Inasmuch

as

the largest

cold

spring

of

this

region

(Cold

Spring)

lies

within

a

mile

of

the

largest

warm

spring

(Warm

Springs),

the

sources

of

their

waters

present

an

interesting

problem.

After a preliminary

inspection

of

the

area,

it

seemed

desirable

to

compare

the

discharge

of

Cold

Spring

with

the

local

rainfall

and

to

obtain

a

continuous

record

of

the

temperature

of

the

water.

The

nature

of

the

diversions

made

this

plan

impossible,

however,

and

in

the

face

of

obvious

disadvantages,

the

necessary

instruments

were

installed

in

a

new

concrete

pool

which

surrounds

North

Spring.

It

was

found

that

the

discharge

of

North

Spring

ranged

from

a

minimum

of

238

gallons

a

minute

early

in

March

1935

to

a

maximum

of

451

gallons

a

minute

on

March

24,

1934.

A

comparison

of

the

curve

of

discharge

with

that

of

local

rain-

fall

as

measured

at

the

Koosevelt

farm

on

Pine

Mountain

(pi.

5)

indicates

that

there

is

a

broad

similarity

in

the

succession

of

highs

and

lows

that

seems

to

be

seasonal.

For

most

of

the

period

of

observation

(December

1933

to

June

30,

1935)

there

seems

to

have

been

a

lag

of

2

or

3

weeks

before

heavy

rainfall

is

reflected in

a

corresponding

rise

in

the

rate

of

discharge

of

the

spring.

Precise

measurements

of

the

temperature

of

numerous

sources

in

the

Cold

Spring

pool

on

November

30,

1933,

showed

that

it

ranged

from

63.4°

to

65°

F.

The

observed

range

during

the

period

of

investiga-

tion

was

from

62.8°

to

65°

F.

At

North

Spring

there

was

no

varia-

tion

in

temperature

in the

pool

on

a single

visit,

and

the

range

through-

out

the

period

was

from

65.3°

to

66.1°

F.

The

combined

discharge

of

South

Springs

nos.

1

and

2

was

about

50

gallons

a

minute,

but

this

was

not

measured

accurately,

as

it

was

one

of

several

minor

contributions

to

Cold

Spring

Branch,

the

discharge

of

which

was

accurately

measured

32

times

during

the

investigation.

The

temperature

of

the

waters

from

the

South

Springs

ranged

from

63.4°

to

64.3°

F.

GEOLOGICAL

STTRVBT

660

WATER-SUPPLY

PAPER

819

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26

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28

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in

2°

HO

HZ

30

a

31

Week

4

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I

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1522

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152229512

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ending

Jan.

Feb.

Mar.

Apr.

May

June

July

Aug.

Sept.

Oct.

Nov.

Dec.

Jan,

Feb. Mar.

Apr.

May

June

1934

1935

RELATION

OF

DISCHARGE

OF

WARM

SPRINGS

TO

RAINFALL

AND

GROUND-WATER

LEVEL

AT

ROOSEVELT

FARM,

JANUARY

1,

1934,

TO

JUNE

30,

1935

Altitude

of

rain

page,

about

1,310

feet?

at

top

of

well,

aboat

1^255

feet.

RAINFALL

ON

ROOSEVELT

FARM

IN

INCHES

DISCHARGE

OF

NORTH

SPRING

IN

GALLONS

PER

MINUTE

g

§

5

<s

'

a

8

'

5J

t>

"*?

z?

COLD

SPRINGS

OF

THE

REGION

13

The

discharge

of

Cold

Spring

Branch

was

measured

intermittently

during

the

first

year

and

weekly

during

the

last

6

months

of

this

in-

vestigation

at

a

point

about

1,500

feet

below

the

lowest

pond in

the

hatchery.

The

measured

discharge

ranged

from

1,282

to

1,822

gallons

a

minute,

and

the

average

was

1,546

gallons.

As

this

includes;

most

of

the

discharge

of

Cold,

North,

and

South

Springs

and

very

little

from

other

sources,

it

is

a

close

approximation

to

the

actual

dis-

charge

of

the

four

springs.

Analyses

of

the

water

from

Cold

Spring

and

North

Spring

appear-

in

the

table

on

page

17.

Trammel's

Spring.

Trammel's

Spring

(no.

9, pi.

2;

see

also pi.

7)

is

about

1,500

feet

southwest

of

Fount

Trammers

house,

west

of

the

Warm

Springs

quadrangle.

It

is

a

circular

pool

about

15

feet

in

diameter

and

2

to

3

feet

deep,

in

swampy

ground

near

the

top

of

the

Hollis

quartzite

that

forms

the

northern

slope

of

Pine

Mountain.

In

December

1933

the

temperature

of

the

water

was

62.2°

F.

and

the

discharge

was

estimated

at

100

gallons

a

minute.

Chemically

the

water

closely

resembles

that

of

Cold

Spring

(17).

Blue

Spring

(no.

8,

pi.

2). Blue

Spring

is

20

miles

southwest

of

Warm

Springs,

on

the

north

slope

of

a

low

ridge

that

forms

the south

side

of

Pine

Mountain.

The

spring

forms

a

nearly

circular

pool

about

25

by

30

feet,

which

occupies

a

recess

in the

quartzite

ridge,

half

sur-

rounded

by

vertical

walls

covered

with

laurel,

ferns,

and

ivy.

The

water

is

quite

clear,

so

that

the

bottom,

25

feet

below

the

surface,

is-

plainly

visible.

The

water

drains

northward

through

a

channel

cut

in

the

rock,

and

measurements

of

discharge

made

weekly

during

the

last

10

months

of

the

investigation

showed

a

range

from

282

gallons

a

minute

(June

13,

1934)

to

367

gallons

(Mar.

22,

1935).

Comparison

of

the

record

of

discharge

with

that

of

the

rainfall

at

West

Point,

15

miles

to

the

northwest,

indicates

that

the

discharge

responds

to

local

rainfall

with

a

lag

that

ranges

from

1

to

3

weeks.

The

temperature

of

the

water

was

64.5°

F.

on

December

8, 1933,

and

64.4°

F.

on

June

14,

1935.

Analyses

of

the

water

at

the

beginning

and

end

of

the

investigation

showed

almost

identical

composition.

The

total

solids,

bicarbonate,

and

silica

content

are

intermediate

between

those

in

most

of

the

cold-

spring

and

warm-spring

waters.

(See

table,

p.

17.)

Cold

chalybeate

springs. At

two localities

hi

the

Warm

Springs

quadrangle

(Chalybeate

and

Oak

Mountain) and

at

one

west

of

its

borders

(White

Sulphur)

iron-bearing

springs

have

been

improved

so

that

the

waters

may

be

used

for

bathing

and

other

purposes.

At

each

of

these

springs

a

hotel

and

cottages

were

maintained

for

many

years,

but

those

at

Chalybeate

were

removed

some

years

ago.

At

Chalybeate,

2

miles

east

of

Manchester,

four

springs

that

lie

in

a

belt

200

feet

long

have

been

improved.

The

waters

of

three

of

these

15458 37 3

14

THE

WARM

SPRINGS

OF

GEORGIA

show

high

total

solids

and

silica

and

appreciable

iron,

and

they

appear

to

be

almost

identical

chemically;

the

total

measured

discharge

has

ranged

from

12

to

24

gallons

a

minute. The

observed

temperature

ranged

from

65.0°

to

65.4°

F.

on

December

8,

1933,

and

from

64.6°

to

64.8°

F.

on

June

14,

1935.

The

fourth

spring,

at

the

east

end

of

the

belt,

yields

water

much

lower

in

total

solids

as

well

as

in

iron.

The

temperature

of

this

spring

was

61.9°

F.

on

December

8,

1933,

and

63.1°

F.

on

June

14,

1935.

Oak

Mountain

Spring

issues

in

a

ravine

on

the

south

slope

of

Oak

Mountain,

where

the

underlying

rocks

are

Manchester

schist.

The

measured

discharge

has

ranged

from

0.54

to

0.94

gallon

a

minute,

and

the

observed,

temperature

from

60°

to

64°

F.

Chemically

the

water

resembles

that

from

the

three

western

springs

at

Chalybeate.

(See

p.

17.)

At

White

Sulphur

Springs

four

sources

have

been

improved White

Sulphur,

Black

Sulphur, Red

Sulphur,

and Chalybeate.

These

springs

issue

in

an

area

of

low

ground

along

State

Highway

18

near

the

crossing

of

Sulphur

Creek,

7

miles

west

of

Warm

Springs.

The

underlying

rocks

are

a

part

of

the

Carolina

gneiss.

The

discharge

of

each

of

these

springs

is

small,

the

range

for

the

four

during

this

in-

vestigation

being from

0.65

to

1.62

gallons

a

minute.

The

tempera-

ture

of

the

water

of

three

of

the

springs

ranged

from

61.9°

F.

on

December

8,

1933,

to

63.1°

F.

on

June

14,

1935;

the

fourth

showed

slightly

higher

temperatures,

possibly

because

it

rises

under

a

dwelling.

Chemically

the

waters

resemble

those

at

Chalybeate.

(See

p.

17.)

Summary of

the

cold

springs.

This

investigation

indicates

that

springs

of

cold

water

that

yield

more

than

50

gallons

a

minute

are

very

rare

in

this

region;

on

the

other

hand,

there

are

many

small

springs

that

yield

1

to

10

gallons

a

minute.

The

high

discharge

of

the

group

of

springs

at

the

fish

hatchery

suggests

that

some

uncommon

circumstances

account

for

their

existence.

(See

pp.

35-36.)

The

improvements

around

the

three

groups

of

chalybeate

springs

give

the

impression

that

they

too

are

very

rare

in

the

region.

The

number

of

areas

where

cold

spring

waters

are

now

depositing

oxides

of

iron

and

the

presence

in

several

areas

of

bodies

of

iron

oxides

large enough

to

justify

mining

operations

indicate

that

chalybeate

springs

are

and

have

been

fairly

widespread.

Both

the

iron

and

the

sulphate

present

in

these springs

indicate

that

the

nearby

rocks

contain

small

amounts

of

disseminated

iron

sulphide,

probably

pyrite.

The

measurements

of

discharge

and

temperature

of

the

chalybeate

springs

indicate

that

they

respond

to

seasonal

rainfall:

the

discharge

is

greatest

and

the

water

temperature

lowest

in

the

late

spring,

after

the

cold

rains

of

late

winter,

and

the

discharge

is

smallest

and

the

water

temperature

highest

during

the

fall,

after

the

months

of

low

rainfall.

THE

WARM

SPRINGS

OF

GEORGIA

15

CHEMICAL

CHARACTER

OF

THE

WATERS

The

waters

of

the

Warm

Springs

region

show

distinct

differences

in

composition

that

correspond

to

differences

in

temperature.

This

is

evident

from

the

analyses

in

the

table

on

pages

17-18

and

from

th6

results

of

a

much

larger

number

of

tests

made

in

the

field.

Analyses

of

samples

taken

from

the

same

spring

at

different

tunes,

however,

show

no

appreciable

changes

in

composition.

The

warm

waters

of

the

region

are

characterized

by

their

content

of

calcium

and

magnesium

bicarbonates,

which,

as

carbonates,

make

up

68

percent

of

the

total

of

120

parts

per

million

of

dry

residue

obtained

by

evaporation

of

the

water.

Silica

makes

up

about

20

percent.

The

preponderance

of

calcium

and

magnesium

bicarbonates

and the

high

proportion

of

silica

set

off

the

warm

waters

as

distinctly

different

from

the

waters

in streams,

in

shallow

wells,

and in

most

of

the

cold

springs

of

the

region.

As

it

is

widely

believed

than

an

appreciable

amount

of

boric

acid

in

water

indicates

a

volcanic

origin,

many

samples

of

both

warm

and

cold

water

were

tested

for boron

by

a

method

which

will

detect

as

small

a

quantity

as

0.1

part

per

million.

None

of

the

samples

re-

sponded

to

the

test.

From

this

evidence

alone,

even

though

the

boron

content

of

the

waters

is

less

than

0.1

part

per

million,

it

is

conceivable

but

improbable

that

a

very

small

part

of

the

water

of

the

warm

springs

is

derived

from

a

volcanic

source.

Typical

cold

water

from

springs,

streams,

or

wells

in

the

Warm

Springs

area

is

characterized

by

its

exceedingly

low

content

of dis-

solved

mineral

matter

which

in

general

is

only

a

little

more

than

one-tenth

that

hi

the

warm

water.

Furthermore,

the

silica

in

the

cold

water

is

about

50

percent

of

the

total

dissolved

material,

although

its

actual

concentration in

parts

per

million

is

only

about

one-third

the

concentration

of

the

silica

in the

typical

warm

water.

The

fact

that

the

warm

waters

generally

contain

about

30

parts

per

million

of

calcium

and

magnesium

together,

whereas

most

of

the

samples

from

cold

springs,

streams, and

shallow

wells

examined

con-

tain

only

about

1

part

per

million,

suggests

that

the

warm

waters

have

had

a

very

different

history

from

most

of

the

cold

waters.

The

composition

of

the

water

from

one

cold

spring Blue

Spring

and

several

streams

suggests

that

it

is

the

normal

cold

water

of

the

region

to

which

has

been

added

a

portion

of

water

like

that

of

the

warm

springs.

On

the

other

hand,

three

springs

at

Chalybeate

and

four

springs

at

White

Sulphur,

the

Oak

Mountain

Spring,

and

the

well

of

the

Manchester

High

School

yield

water

that

is

intermediate

in

several

respects

but

in others

cannot

be

considered

a

mixture

of

typical

warm

and

cold

waters.

In

their

content

of

calcium,

magne-

sium,

and

bicarbonate

they

fall

between

the

typical

warm

and

cold

16

THE

WARM

SPRINGS

OF

GEORGIA

springs

but

are

nearer

the

warm

springs.

Their

sulphate

content,

however,

is

about

\%

to

2

times

the

sulphate

content

of

the

warm-

spring

waters

and

from

5

to

10

times

that

of

typical

cold-spring

waters.

Even

so,

the

sulphate

makes

up

only

about

10

percent

of

the

mineral

content

of

these

intermediate

waters.

The

calcium,

magnesium,

and

carbonate

account

for

more

of

the

residue

on

evapo-

ration

of

the

waters

than

all

the

other

constituents.

The

total

quan-

tity

of

dissolved

mineral

matter

in

these

intermediate

waters

is

about

the

same

as

is

found

in

the

warm

waters,

but

the

silica

content

is

nearly

double

that

of

the

warm-spring

waters,

both

in

parts

per

mil-

lion

and

as

percentages

of

the

dried

residue

on

evaporation.

Some

of

the

intermediate

waters

contain

much

more

iron

than

is

found

in

the

other

waters

of

the

area,

and

one,

White

Sulphur,

contains

hydrogen

sulphide.

It

seems

probable

that

the

history

of

these

intermediate

waters

must

be

different

from

the

history

of

the

typical

warm or

cold

waters

of

the

area.

The

accompanying

table

of

analyses

shows

the

amounts

of

constit-

uents

that

were

found

in

measurable

quantities

and

is

followed

by

brief

descriptions

of

the

sources

of

the

samples

analyzed.

All

the

samples

were

tested

for

carbonate,

and

none

was

found.

No

boric

acid

was

found

in

the

samples

tested

for

this

constituent.

A

few

of

the

samples

from

warm

springs

were

tested

for

manganese,

and

none

was

found.

The

table

does

not

give

the

results

of

these

tests

for

carbonate,

boric

acid,

and

manganese.

Analyses

of

spring,

stream,

and

wett waters

in

and

near

Warm

Springs,

Qa.

[Analyzed

by

W.

L.

Lamar,

except

no.

41.

Analyses

given

in

parts

per

million]

No.

1

2

3

4

4A

a

6

7

8

9

10

11

12

IS

14

15

16

17

is

19

9,0

91

22

WABM

SPEINGS

Warm

Springs:

Bast

source

........

... ...

Parkman

Spring

__________

Brown's

Spring

___________

ing

Spring

_____________

Barker

Spring

___________

Taylor

Spring

___________

COLD

SPEINGS

Blue

Spring

____________

Trammel's

Spring

___

.

_

.

_

Cold

Spring

__

......

..............

Chalybeate

Spring

No.

1.

_____

Chalybeate

Snrine

No.

3

__

-

Date

of

col-

lection

/Dec.

11,1933

\June

13,1935

/Dec.

11.1933

\June

13,1935

Dec.

10,1933

Dec.

8, 1933

June

14,1935

Apr.

2,

1934

June

12,1935

Apr.

2,

1934

June

12,1935

Mar.

23,

1934

June

12,1035

__

do

____

June

15,1935

/Deo.

8,1933

\June

14,1935

Dec.

9,1933

Dec.

10,1933

June

13,1935

Dec.

10,1933

Mar.

31,

1934

June

13,1935

Deo.

10,1933

June

13,1935

Dec.

8,1933

.. do .-..

.....

do

._.

Dec.

7,

1933

Dec.

8,1933

..

_

do

___

.

/Dec.

8,

1933

\June

14,1935

Dec.

8,1933

.

do

. .

Tem-

perature

(°F.)

88.0

O/.

/

87.4

O<*

A

76.6

69.0

74.2

/O.

V

72.6

71.9

73»4

1

9t

O

78.5

74.8

64.5

64.4

62.2

63.4-65.0

OO.

V-VTU

a

66.1

65.6

64.3

DO.

v

62.5

62.2

63.8

66.4

62.6

59.0

62.8

65.2

65.4

65.0

Total

dis-

solved

solids

121

J.A>

117

120

114

144

A*n

66

83

107

141

105

43

45

14

18

17

14

16

141

15

109

126

Silica

(SiOj)

23

21

24

21

25

*O

14

16

18

16

£iQ

30

20

12

14

7.6

7.3

/.

V

9.4

9.0

6.8

46

8.0

38

41

45

Iron

(Fe)

0.01

.01

.02

.01

.03

.02

.01

.04

.01

.02

.01

.02

.01

.02

.01

8.0

3.4

A.

O

Cal-

cium

(Oa)

21

41

20

19

27

At

9.9

10

14

W

L0

23

18

5,0

5.5

.2

.4

.5

.7

.6

.3

.7

17

.2

8.6

12

La

Mag-

nesium

(Mg)

12

L£

11

10

11

5.7

5.9

7.6

11

10

2.9

V

.3

.4

.3

.4

3.2

.3

5.4

5.3

Sodi-

um

(Na)

1.6

1.7

2.6

2.8

. 1

2.1

.

o

2,4

2.4

.

O

7.4

2.9

2.1

H

1.1

1.0

1.4

1.5

JL*

a

16

1.5

8.3

8.5

o.

o

Potas-

sium

(K)

3.6

3.5

.

*

2.5

4.3

4.4

2.0

.

O

2.4

3.4

3.2

1.9

1.1

1.5

.5

.2

.4

.5

.7

.2

.4

2.0

.4

3.4

3.3

.

^

Bicar-

bonate

(HCOa)

118

114

115

111

144

±*O

61

84

82

114

137

111

31

o<£

3.0

2.0

4.0

3.5

4.4

3.0

u

100

97

96

2.0

58

81

oi

83

82

Sul-

phate

(SOO

7.3

/.

0

7.0

7.4

5.1

4.9

5.1

3.0

.

U

3

4.0

4,4

*

O

5.6

4.1

1.9

ifi

1.2

1.1

.7

1.4

.8

1.2

a

6.0

6

1.1

1

13

10

tf.

O

10

Chlo-

ride

(01)

1.8

2.0

1.8

O

2

1.8

1.5

1.8

1.6

1.8

U

1.6

1.4

1.5

1.4

1.5

1.4

1.5

2.1

2

1.8

2.4

1.8

1.9

2

Fluo-

ride

(F)

0.1

.1

0

.1

0

.3

.0

.6

.1

.0

Ni-

trate

(NO,)

0.10

.15

.05

0

AA

0

.05

0

.05

0

.15

0

.05

AA

0

.05

AK

0

.06

.43

.

o*

0

.0

.05

AQ

Total

hard-

ness

as

CaOOi

102

95

93

108

48

66

93

103

86

24

26

1.7

2.2

2

t

3.4

2.7

2.4

U

56

1.7

44

62

Kfi

Analyses

of

spring,

stream,

and

well

waters

in

and

near

Warm

Springs,

Oa.

Continued

No.

as

?4

?f>

36

w

29

30

31

33

38

34

35

36

37

38

39

40

41

COLD

SPRINGS

continued

Woodbury

Spring

No.

1

............

SURFACE

WATEES

Do

.--- .- '

Mountain

stream

(about

4

miles

south

of

Shiloh,

Ga.)_.

_

.

.......

Do....-

....

......

Manchester

reservoir..

.............

Mountain

stream

on

Pine

Mountain.

WELLS

Date

of

col-

lection

Dec.

8. 1933

Mar.

24,

1934

Apr.

2,

1934

.. do. ....

-..-do........

June

15,1935

..do

.....

Dec.

9,

1933

Dec.

7,

1933

Mar.

29,

1934

Dec.

9,

1933

Dec.

10,1933

Apr.

2,

1934

Dec.

11,1933

Mar.

28,

1934

July

23,1929

Tem-

perature

(°F.)

61.9

54.0

63.6

64.3

48

55

57

50

53

63

47

46

64

59.5

Total

dis-

solved

solids

18

16

15

19

so

23

37

15

23

33

103

Silica

(SiOj)

6.9

8.3

7.5

4.5

5.8

14

8.2

14

5.0

5.8

9.8

43

Iron

(Fe)

.01

.02

.04

.02

.25

.20

.41

.06

1.7

.01

.25

Cal-

cium

(Oa)

.3

.5

2.1

.8

1.6

.3

1.5

.5

13

Mag-

nesium

(Mg)

.3

.4

1.2

.6

.9

.3

1.4

1.3

2.5

Sodi-

um

(Na)

1.5

1.4

1.6

3.1

1.0

3.2

1.9

1.7

2.3

7.3

Potas-

sium

(K)

.5

.6

.2

1.6

.4

1.1

.2

.5

3.2

Bicar-

bonate

(HC0

3

)

15

2

A

2.0

6.0

3.0

n

r\

3.0

17

3.0

14

29

2.0

11

31

4.0

2.0

59

Sul-

phate

(S0

4

)

2

C

1.6

1.8

1.6

2

1.6

1.4

2

1.8

4.1

Chlo-

ride

(01)

4

1

1.8

1

2.1

1.6

2.0

2.1

2

2.1

2.2

2

3.0

4.6

2

Fluo-

ride

(F)

.0

.6

.0

Ni-

trate

(NOs)

.6

1.3

.28

.05

.22

.05

.07

.06

.15

.05

.0

.18

6.8

Total

hard-

ness

as

CaCOj

2.0

2.9

9

n

2.9

10

4.5

7.7

2.0

9.5

6.6

43

00

CHEMICAL

CHARACTER

OF

THE

WATERS

}g

1.

Warm

Springs,

the

springs

for

which

the

town

of

Warm

Springs,

Ga.,

is

named;

location

shown

on

plate

2;

owned

by

Warm

Springs

Foundation.

This

source

supplies

much

the

largest

quantity

of

water

of

all

the

warm

springs

in

the

region,

and

its

temperature

is

the

highest.

It

supplies

the

pool

used

in

the

treat-

ment

of

patients

at

the

Warm

Springs

Foundation.

2.

Parkman

Spring;

in

Parkman

Pond,

2.6

miles

southeast

of

Warm

Springs;

owned

by

W.

G.

Harry.

The

sample, collected

when

the

pond

was

drained

to

a

low

level,

probably

contained

some

surface

water,

because

a

stream

was

flowing

over

the

spring

outlet.

3.

Brown's

Spring;

4

miles

in

an

air

line

east-northeast

of

Manchester,

Ga.;

owned

by

Tom

Brown.

Water

issues

from

the

ground

at

three

distinct

sources;

the

sample

was

collected

from

the

source

having

the

largest

flow.

4.

Thundering

Spring;

in

a

small

pond

5.1

miles

in

an

air

line

east-southeast

of

Woodbury,

Ga.

The

sample

was

collected

directly

from

the

main

source

in

about

the

center

of

the

pond

but

may

contain

some

creek

water,

as

the

pond

is

also

fed

by

a

creek.

4A.

Small

spring

tributary

to

Thundering

Spring;

5.2

miles

in

an

air

line

east-

southeast

of

Woodbury,

Ga.

5.

Barker

Spring;

on

State

Highway

74,

about

7

miles

west-northwest

of

Thomaston,

Ga.;

owned by

Barker

estate. The

spring

issues

in

a

swimming

pool.

6.

Lifsey

Spring;

about

5

miles

south

of

Zebulon,

Ga.;

owned

by

John

Mangham.

The

spring

issues

in

a

swimming

pool

200

feet

north

of

a

county

road

that

extends

westward

from

Pine

Mountain

Store,

on

U.

S.

Highway

19.

7.

Taylor

Spring;

6.5

miles

south

of

Zebulon,

on

U.

S.

Highway

19;

owned

by

R.

G.

Gibson.

The

sample

was

collected

at

the

swimming-pool

intake,

at

the

lower

end

of

the

reservoir

fed

by

the

spring.

8.

Blue

Spring;

about

5

miles

west-southwest

of

Hamilton,

Ga.;

owned

by

C.

J.

Galloway.

The

spring

forms

a

deep

pool.

9.

Trammers

Spring;

6.1

miles

in

an

air

line

west-southwest

of

Warm

Springs,

Ga.;

owned

by

Fount

Trammel.

10.

Cold

Spring;

Warm

Springs,

Ga.;

owned

by

U.

S.

fish

hatchery.

The

spring

issues

in

a

covered

reservoir

on

State

Highway

41.

Source

of

public

supply

for

town

of

Warm

Springs.

11.

North

Spring;

Warm

Springs,

Ga.;

owned

by

U.

S.

fish

hatchery.

The

spring

issues

in

an

open

reservoir

on

State

Highway

41.

12.

South

Spring

No.

1;

on

State

Highway

41,

Warm

Springs,

Ga.;

owned

by

U.

S.

fish

hatchery.

13.

White

Sulphur

Spring;

White

Sulphur

Springs,

Ga.;

owned

by

Mrs.

N.

E,

Goodman.

The

spring

is

covered

and

discharges

from

a

pipe

into

a

small

pool.

14.

Black

Sulphur

Spring;

White

Sulphur

Springs,

Ga.;

owned

by

Mrs.

N.

E.

Goodman.

15.

Red Sulphur

Spring;

White

Sulphur

Springs,

Ga.;

owned

by

Mrs.

N.

E.

Goodman.

16.

Chalybeate

Spring;

in

a

roadside

store

at

White

Sulphur

Springs,

Ga.;

owned

by

Mrs.

N.

E.

Goodman.

17.

Kings

Gap

Spring;

8.2

miles

in

an

air

line

west-southwest

of

Warm

Springs,

Ga.

The

spring

issues

in

a

covered

reservoir;

source

of

public

supply

for

Chip-

ley,

Ga.

18.

Pine

Mountain

Spring;

on

U.

S.

Highway

27,

Hog

Gap,

Ga.

19.

Oak

Mountain

Spring;

about

4

miles

south

of

Shiloh,

Ga.

The

spring

is

covered

and

discharges

through

a

pipe.

20.

Chalybeate

Spring

No.

1;

Chalybeate

Springs,

Ga.;

owned

by

W.

A.

Reeves.

20

THE

WARM

SPRINGS

OF

GEORGIA

21.

Chalybeate

Spring

No.

2;

Chalybeate

Springs,

Ga.;

owned

by

W.

A.

Reeves.

22.

Chalybeate

Spring

No.

3;

Chalybeate

Springs,

Ga.;

owned

by

W.

A.

Reeves.

23.

Chalybeate

Spring

No.

4;

Chalybeate

Springs,

Ga.;

owned

by

W.

A.

Reeves.

24.

Small

spring;

4

miles

in

an

air

line

east-northeast

of

Manchester,

Ga.;

owned

by

Tom

Brown.

This

spring

is

close

to

Brown's

Spring

(no.

3).

25.

Gill

Spring;

3

miles

in

an

air

line

south

of

Woodbury,

Ga.;

owned

by

W.

R.

Gill.

The

sample

was collected

from

the

largest

of

three

separate

springs.

26.

Woodbury Spring

No.

1;

the

larger

of

two

springs

2.9

miles

in

an

air

line

south

of

Woodbury,

Ga.;

owned

by

town

of

Woodbury.

Source

of

public

supply

for

Woodbury.

27.

Woodbury

Spring

No.

2;

the

smaller

of

two

springs

2.9

miles

in

an

air

line

south

of

Woodbury,

Ga.;

owned

by

town

of

Woodbury.

28.

Willingham

Spring

No.

1;

about

7.5

miles

northwest

of

Thomaston,

Ga.;

owned

by

W.

F.

Ellerbee.

One

of

three

springs

made

up

of

numerous

small

seeps.

The

sample

was

collected

from

the

spring

east

of

the

other

two.

29.

Cascade

Branch;

1.5

miles

in

an

air

line

southwest

of

Warm

Springs,

Ga.

Sample

collected

at

road

crossing.

30.

Mount

Hope

Branch;

2.4

miles

in

an

air

line

west-southwest

of

Warm

Springs,

Ga.

Sample

collected

at

road

crossing.

31.

Mountain

stream

on

Pine

Mountain;

8.2

miles

on

an

air

line

southwest

of

Warm

Springs,

Ga.

Sample

collected

at

Shiloh-Chipley

road

crossing.

32.

Mountain

stream

on

Pine

Mountain;

6.3

miles

in

an

air

line

southwest

of

Warm

Springs,

Ga.

Sample

collected

from

west

branch

just

above

confluence

with

east

branch

at

Shiloh-Chipley

road

crossing.

33.

Sparks

Creek;

4.5

miles

in

an air

line

south-southwest

of

Warm

Springs,

Ga.

Sample

collected

from

east

branch

just

above

confluence

with

west

branch

at

Shiloh-Chipley

road

crossing.

34.

Mountain

stream;

about

4

miles

south

of

Shiloh,

Ga.

Sample

collected

near

the

swimming

pool

in

the

Oak

Mountain

Spring

resort.

35.

Mountain

stream;

about

4

miles

south

of

Shiloh,

Ga.

Sample

collected

in

the

Oak

Mountain

Spring

resort

at

a

point

about

150

feet

upstream

from

Oak

Mountain

Spring.

36.

Manchester

reservoir;

2.7

miles

in

an air

line

south

of

Warm

Springs, Ga.

Source

of

public

supply

for

Manchester,

Ga.

Sample

collected

from

reservoir

on

headwaters

of

Pigeon

Creek

above

Cooler

Branch.

37.

Mountain

stream

on

Pine

Mountain;

2.6

miles

in

an

air

line

southeast

of

Warm

Springs,

Ga.

The

stream enters

Parkman

Pond

from

the

northwest.

Sample

collected

just

above

Parkman

Pond

and

above

Parkman

Spring

(no.

2),

which

is

located

in

the

pond.

The

sample

collected

from

Parkman

Spring

prob-

ably

contained

some

of

this

surface water.

38.

Mountain

stream;

5.2

miles

in

an

air

line

east-southeast

of

Woodbury,

Ga.

This

stream

is

tributary

to Thundering

Spring.

Sample

collected

about

50

feet

below

the

confluence

of

two

small

streams

and

above

all

sources

of

warm

water.

Warm

waters

from

springs

enter

this

stream

below

the

point

at

which

this

sample

was

collected.

39.

Well

27

feet

deep;

Warm

Springs,

Ga.;

owned

by

J.

E.

Mathis.

40.

Well

35

feet

deep;

2

miles

in

an

air

line

east-northeast

of

Shiloh,

Ga.;

owned

by

E.

A.

Fuller.

41.

Well

530

feet

deep,

drilled

in!928;

on

the

Manchester

High

School

grounds

on

State

Highway

41,

Manchester, Ga.;

owned

by

city

of

Manchester.

The

well

is

used

as

an

emergency

source

for

the

Manchester

public

supply.

(See

no.

36.)

Analysis

furnished

by

the

city

commissioners

of

Manchester.

GEOLOGICAL

8TJBVET

4

WATEB-STJPPLY

PAPEB

819

PLATE

0

A

/\

Ellers

S

\

rson

well

V

Rons

30.

B

_F«!eb

cr

Butt

ending

4llieZ5l

8

I5Z2

I

SISZZZaS

I2I9263IO!7243I7

I4ZI28

5

1219262

9

1623306

BZOZ74III8Z5I

815222961320273

10172431?

I4ZI287I42I284II

18252

3

I6Z330

6

I320^7

Jan.

Feb.

Mar.

Apr.

May

June

July

Aug.

Sept.

Oct

Nov.

Dec.

Jan.

Feb.

Mar.

Apr.

May

June

1934

"

1935

FLUCTUATIONS

OF

GROUND-WATER

LEVEL

IN

FOUR

WELLS

AND

RELATION

TO

RAINFALL,

EASTERN

PART

OF

PINE

MOUNTAIN

AREA.

OTHER'

HYDR0LOGIC

INVESTIGATIONS

GA3E3

IN

THE

SPRING

WATERS

21

Small

quantities

of

gas

rise

from

most

of

the

springs

of

the

region,

both

warm

and

cold.

Duplicate

samples

for

analysis

were

collected

rfrom

Warm,

Thundering,

Cold,

and

North

Springs.

The

analyses,

made

by

W.

P.

Yant,

of

the Bureau

of

Mines

at

Pittsburgh,

Pa.,

are

given

in

the

subjoined

table,

with

an

analysis

of

air

for

comparison.

The

gases

from

the

two

cold

springs

(Cold

and

North

Springs)

are

essentially

air

in

which

between

2

and

3

percent

of

oxygen

has

been

Teplaced

by

carbon

dioxide.

The

gas

from

Thundering

Spring

is

nearly

unmodified

air;

that

from

Warm

Springs

contains

7

percent

less

oxygen

than

is

found

in

air

and

correspondingly

more

nitrogen.

A

large

content

of

carbon

dioxide

in

a

spring

water

has

been

held

T>y

some

authorities

to

indicate

a

volcanic

origin

of

the

water.

The

small

amount

of

carbon

dioxide

in

the

gases

from

both

Thundering

Spring

and

Warm

Springs

may

thus

be

considered

indicative

of

a

meteoric

rather

than

a

volcanic

origin

of

the

water

of

the

warm

springs

>of

this

region.

Indeed,

the

highest

content

of

carbon

dioxide

is

found

in

the

gas

from

the

largest

cold

spring.

Analyses

of

gases

from

springs

in

Warm

Springs

district,

Georgia

[Samples

collected

by

W.

L.

Lamar,

Geological

Survey.

Analyses

by

W.

P.

Yant,

Bureau

of

Mines]

Laboratory

no

_______

"Nitrogen

1...

___

.

___

Total

.................

Warm

Springs

58705

85.50

13.91

.59

0

100.00

Mar.

3

58706

85.19

14.26

.55

0

100.00

1,

1934

Thundering

Spring

58703

79.01

20.87

.12

0

100.00

Apr.

1

58704

78.97

20.91

.12

0

100.00

2,1934

Cold Spring

58709

79.

69

18.01

2.30

0

100.00

Mar.

3

58710

79.72

18.00

2.28

0

100.00

1,1934

North

Spring

58707

79.66

17.70

2.64

0

100.00

Mar.

3

58708

79.77

17.63

2.60

0

100.00

1,1934

Air

79.

059

20.94

i

Including

argon

and

other

rare

gases.

OTHER

HYDROLOGIC

INVESTIGATIONS

The

distribution,

environment,

discharge,

chemical

character,

and

temperature

of

the

spring

waters

of

the

region

have

been

set

forth

In

the

preceding

pages.

In

order

to

throw

light

on

the

sources

of

the

waters

that

issue

from

the

several

warm

springs

and

from

the

large

springs

called

Cold Spring,

a

comprehensive

program

of

study

and

systematic

measurements

was

carried

out

between

October

1,

1933,

and

June

30,

1935.

Special

attention

was

given

to

the

rainfall,

water

levels

in

wells,

and

discharge

of

streams

in

an

area

of

32

square

miles

along

Pine

Mountain,

here

referred

to

as

the

Pine

Mountain

area

(pis.

7,

8).

About two-thirds

of

this

area

lies

within

the

Warm

22

THE

WARM

SPRINGS

OF

GEORGIA.

Springs

quadrangle,

and

one-third

lies

west

of

it.

In

order

to

deter-

mine

the

approximate

quantity

of

water

that

falls

on

this

area,

rain

gages

were

installed

on

the

Roosevelt

and

Trammel

farms,

as

indi-

cated

on

plate

7.

Daily

readings

were

made

at

the

Roosevelt

gage,

and

weekly

readings

at

the Trammel

gage.

The

United

States

Weather

Bureau maintains

five

stations

within

35

miles

of

the

area.

To

obtain

information

concerning

the

level

of

the

ground

water

and

its

temperature,

four

quarterly

observations

were

made

at

36

wells

in

the

low

country

that

surrounds

the

Pine

Mountain

area,

and

observations

were

made

weekly

from

December

1933

to

June

30

r

1935,

at

six

other

wells.

To

determine

the

distribution

of

run-off

from

the

Pine

Mountain

area,

measurements

were

made

of

the

discharge

from

30

drainage

basins

in

the

area.

A

gaging

station

was

installed

on

Mill

Creek

r

which

is

the

most

accessible

of

the larger

streams,

and

a

continuous-

record

of

discharge

was

obtained

from

January

1,

1934,

to

June

30

r

1935.

At

selected

stations

on

the

other

29

streams,

measurements

of

discharge

were

made

intermittently

over

the

same

period.

RAINFALL

The

following

table

shows

the

monthly

rainfall

from

January

1934

to

June

1935,

recorded

by

the

gages

on

the

Roosevelt

and Trammel

farms

and

at

the

stations

maintained

by

the

United

States

Weather

Bureau

at

Columbus,

West

Point,

Woodbury,

and

Talbotton.

The

weekly

rainfall

at

the

Roosevelt

farm

is

shown

graphically

on

plates

4,

5,

and

6.

Monthly

rainfall,

in

inches,

in

or

near

the

Pine

Mountain

area

1934

June

July

...........

November

Total....

......................

.

1935

March

April..

.-_....

........

...............

-

.

May

Total.....

.......................

Roosevelt

farm

'

4.72

1.89

4.42

2

63

.99

1.99

45.

99

1.74

2.62

6.69

2

Q7

Trammel

farm

1

4.74

5.36

2.81

3.44

8.19

Q

97

.84

1.25

2.23

43.97

1.99

3.00

7.96

4.35

2.77

22.78

Colum-

bus

2

3.27

3.78

6.10

4.21

2.40

4.24

4.29

4.25

.40

1.33

2.47

39.94

1.83

2.61

6.13

4.15

2.30

2.63

19.65

West

Point

2

1.83

4.86

4.83

6.02

3.63

6.30

4.15

6.32

1.84

2.67

57.18

2.22

4.09

6.84

3.76

4.17

24.69

Wood-

bury

2

3.17

4.71

5.57

2.44

9.78

3.64

5.48

4.67

3.84

1.25

2.74

52.07

1.96

2.49

6.72

2.92

2.42

3.95

20.46

Talbot-

ton

i

4.19

7.36

6.23

4.15.

8.05

4.66

1.53

3.19

1.38

3.38.

1.73

2.54

7.85

3.07

3.37

3.12

21.68

1

Gages

installed

and

maintained

during

this

investigation.

2

Records

of

U.

S.

Weather

Bureau.

OTHER

HYDROLOGIC

INVESTIGATIONS

23

WATER

LEVELS

IN

WELLS

The

records

of

water

levels

that

were

obtained

in

six

wells

on

and

near

Pine

Mountain

indicate

that

in

the

lowlands,

where

the

ground-

water

table

is

generally

near

the

surface,

it

rises

immediately

and

abruptly

after

rains,

whereas

on

Pine

Mountain,

where

the

water

table

lies

at

greater

depths,

it

rises

slowly

after

rams

and

the

rise

is

relatively

less

than

in

the

lowlands

(pi.

6).

It

seems

significant

that

the

fluctuations

of

the

water

table

in

the

well

on

the

Roosevelt

farm,

which

is

sunk

in

the

lower

200

feet

of

the

Hollis

quartzite,

resemble

those

of

the

local

rainfall,

but

2

to

5

weeks

seems

to

elapse

before

high

rainfall

is

reflected

in

a

rise

in

the

local

water

table.

Both

curves

resemble

that

of

the

discharge

of

Warm

Springs,

in

which

high

dis-

charge

lags

6

or

7

weeks

behind

high

rainfall

(pi.

4).

STREAMS

In

the

hope

that

a

close

study

of

the

run-off

from

the

basins

of

the

Pine

Mountain

area

might

reveal

deficiencies

or

great

differences

that

would

aid

in

determining

the

source

of

the

waters

that

issue

at

Cold

and

Warm

Springs,

a

program

of

measurement

of

the

discharges

of

the

streams

was

undertaken.

The

30

drainage

basins

of

the

Pine

Mountain

area

are

shown

on

plates

7

and

8.

They

range in

area

from

44

to

2,520

acres;

11

basins

lie

south

of

the

crest

of

Pine

Mountain,

and

19

lie

north

of

it.

There

are

obvious

differences

in

the

form

and

other

features

of

these

basins

that

are

determined

largely

by

the

nature

and

attitude

of

the

under-

lying

rocks.

The

north

slope

of

Pine

Mountain

is

underlain

by

the

sheet

of

Hollis

quartzite

(fig.

1),

700

to

800

feet

thick,

which,

except

for

several

minor

folds,

dips

gently

north.

The

streams

that

flow

north

and

east

from

the

Pine

Mountain

divide

rise

in

small

swampy

areas

that

lie

at

the

junction

of

several

ravines.

As

they

leave

the

Pine

Mountain

area

most

of

them

flow

through

narrow

V-shaped

notches

cut

in

the

quartzite.

There

are

some

clearings

on

the

north

slope,

but

most

of

the

area

is

still

covered

with

the

native

forest.

Considerable clearing

has

been

done

in

the

eastern

basins.

For

most

of

its

length

within

this

area

Pine

Mountain

presents

a

steep

escarpment

toward

the

south,

and

the

basins

that

drain

south

are

largely

cut

in

the

Woodland

gneiss,

which

underlies

the

Hollis

quartzite.

Almost

half

of

the

area

within

these basins

is

cleared

and

cultivated.

The

streams

rise

in

timbered

swampy

areas

near

the

heads

of

the

basins.

So

far

as

possible,

the

discharge

of

all

the

streams

wa&

measured

where

they

were

crossed

by

the

county

roads

that

follow

the

base

of

the

mountain

on

its

north

and

south

sides.

The

geologic

study

of

Pine

Mountain

indicates

that

for

most

of

its-

length

the

divide

that

separates the

underground

water

which

flow&

north

from

that

which

flows

south

probably

lies

a

few

hundred

feet

24

THE

WARM

SPRINGS

OF

GEORGIA

south

of

the

topographic

divide

on

the

surface.

In

other

words,

if

all

other

influences

that

affect

the

stream

discharges

were

the

same,

.the

average

discharge

per

unit

of

area

from

the

northern

drainage

basins

should

be

a

little

greater

than

that

from

the

southern

basins.

In

order

to

obtain

data

concerning

the

discharge

of

the

streams,

the

following

procedure

was

adopted.

As

the

funds

available

did

not

permit

installation

of

gages

on

all

the

streams,

it

was

decided to

install

a

continuously

recording

gage

on

one

large

stream,

Mill

Creek,

which

drains

an

area

of

556

acres,

and

to

make numerous

intermittent

measurements

of

discharge

on

the

other

streams.

For

streams

that

discharged

less

than

200

gallons

a

minute,

a

small

venturi

flume

was

used;

for

larger

streams,

a

current

meter

was

used

at

a

place

of

simple

cross

section.

During

the

period

July

1,

1934,

to

June

30,

1935,

dis-

charge

of

the

larger

streams

was

measured

20

to

25

times;

that

of

the

smaller

streams,

11

to

15

times.

For

each

measurement

the

ratio

of

the

discharge

of

the

stream

to

that

of

the

control

stream,

Mill

Creek,

on

the

same

day

was

calculated.

The

average

of

these

ratios

was

assumed

to

represent

the

ratio

of

the

discharge

to

that

of

Mill

Creek

over

the

entire

year.

As

the

data

of

these

measurements

of

Mill

XDreek

and the

other

streams

are

voluminous, only

the

significant

results

are

presented

here;

details

will

be

given

in

the

final

report.

As

a

check,

the

distribution

of

discharge

was

determined

for

a

short

period

late

in

March

1934

and

for

the

year

July

1,

1934,

to

June

30,

1935.

Plate

7

shows

the

drainage

basins,

their

area,

and

the

discharge

of

their

streams,

in

gallons

per

minute

per

acre,

during

the

short

period

late

in

March

1934.

It

reveals

some

interesting

features.

It

shows

that

there

is

considerable

similarity

in

the

run-off

per

acre

of

the

basins

that

drain

southward

from

the

Pine

Mountain

divide.

If

the

run-off

from

five

small

basins

(nos.

25, 26, 27,

28,

29)

is

combined,

because

their

separate

drainage

divides

cannot

be

placed

accurately

on

the

only

map

available,

the

range in

run-off

was

from

0.50

to

0.90

gallon

per

minute

per

acre,

and

only

one

exceeded

0.64

gallon.

The

average

run-off

from

the

11

basins

that

lie

south

of

Pine

Mountain

was

0.66

gallon

per

minute

per

acre.

The

run-off

of

the

basins

that

lie

on

the

north

side

of

Pine

Mountain

showed

a

much

wider

range.

It

is

noteworthy

that

most

of

the

basins

that

lie

within

3

miles

west

and

southwest

of

Warm

Springs

discharged

much

less

than

the

average,

and

that

except in

time

of

storms,

no

surface

water

leaves

the

two

basins

that

lie

south

of

Warm

and

Cold

Springs.

The

average

run-off

of

all

the

basins

on

the

north

slope,

exclusive

of

the

discharge

of

the

Warm

and

Cold

Springs,

was

0.54

gallon

per

minute

per

acre.

If

to

the

discharge

of

the

streams

there

is

added

the

discharge

of

Cold

Spring

Branch

during

this

period

(1,672

gallons

per

minute),

the

average

discharge

was

0.66

gallon

per

minute

GEOLOGICAL

8TJEVET

WATEK-StTPPLY

PAPER

819

PLATE

7

84°45'

Average

discharge

of

a//

streams

north

of

Pine

Mountain

Divide

_

North

of

Pine

Mountain

Divide

inc/uding

Cofd

Springs

GALLON

PER.

MIN-

u

TE

f

3

^

A

CfZE

......

O.54

O.66

North

of

Pine

Mountain

Divide

including

Co/d

Springs

and

Warm

Springs

1

0

L

1

I I

1

I

1

i

O.

73

Mil1

Creek

gaging

xta.

5O7

SL,

etc.,

area,

in acres

Warm

Springs

31

aD/schorge

3

Miles

Average

discharge

of

crff

streams

south

of

Pine

Mountain

Divide

O.66

gct//on

per

minute

per

acr&

32^

50

84°45'

OUTLINE

MAP

OF

PINE

MOUNTAIN

DRAINAGE

BASINS

SHOWING

STREAM

DISCHARGE,

IN

GALLONS

PER

MINUTE

PER

ACRE, MARCH

12,

13, 14,

23,

1934.

Numbers

indicate location

of

stream-gaging

stations.

GEOLOGICAL SURVEY

WATER-SUPPLY

PAPER

819

PLATE

8

84*45

GALLON

PER

MIN-

Averape

discharge

ofa//^

streams

U

T£

PE*

ACRE

north

of

Pine

Mountain

Divide

_______

O.3I

Norih

of

Pine

Mountain

D/w'de

inc/udiny

Co/d

Spring's

0.43

,

507

a,

etc.,

area

/n

acres

Warm

Springs

North

of

Pine

Mountain

D/'v/de

fftc/udingr

Co/d

Sprt'ngs

and

Warm

Spr/n<ps

_:

Aver

acre

for

stations

BS

to

29

inclusive

(993

tares)

is

O.4O.

Average

discharge

of

a//

streams

south

ofP/ne

Mountain

Div/de

O.44

get,//on

per

minute

per

acre

OUTLINE

MAP

OF

PINE

MOUNTAIN

DRAINAGE

BASINS

SHOWING

STREAM

DISCHARGE,

IN

GALLONS

PER

MINUTE

PER

ACRE,

JULY

1,

1934,

TO

JUNE

30,

1935.

Numbers

indicate

location

of

stream-gaging

stations.

ROCK

FORMATIONS

25

per

acre,

a

figure

that

coincides

with

the

average

discharge

of

the

basins

south

of

the

divide.

The

"Warm

Springs

also

rise

on

the

northern

border

of

the

Pine

Mountain

area,

however,

and

if

their

discharge

during

this

period

(617

plus

288,

or

905

gallons

per

minute)

is

added

to

that

of

the

streams

and

Cold

Spring

Branch,

the

average

discharge

was

0.73

gallon

per

minute

per

acre.

For

the

longer

period July

1,1934,

to

June

30,1935 the

range

in

average

run-off

from

the

several

basins

was

not

so

great

as

it

was

for

the

short

period.

(See

pi.

8.)

For

the

basins

that

lie

south

of

the

Pine

Mountain

divide,

the

average

run-off

for

the

year

was

0.44

gallon

per

minute

per

acre.

For

the

basins

north

of

the

divide,

the

average

run-off

was

0.31

gallon

per

minute

per

acre.

If

to

the

run-off

is

added

the

average

discharge

of

Cold

Spring

Branch

for

the

period

(1,546

gallons

per

minute),

the

average

discharge

for

all

of

the area

north

of

the

divide

was

0.43

gallon

per

minute

per

acre.

If

the

dis-

charge

of

all

the

springs

of

the

Warm

Springs

area

(887

gallons

per

minute)

is

included

in

the

total,

the

average

discharge

was

0.51

gallon

per

minute

per

acre.

These

data

for

both

the

short

and

long periods

indicate

1.

That

the

streams

that

drain

the

basins

north

of

the

Pine

Moun-

tain

divide

discharge

less

water

per

minute

per

acre

than

those

that

drain

the

basins

south

of

the

divide.

2.

That

if

the

discharge

of

Cold

Spring

Branch

is

added

to

that

of

the

other

streams

north

of

the

divide,

the

total

expressed

in

gallons

per

minute

per

acre

approximately

equals

the

average

of

the

streams

south

of

the

divide.

,

3.

That

if,

to

the

discharge

of

the

streams

north

of

the

divide

and-

Cold

Spring

Branch,

there

is

also

added

the

discharge

of

the

springs

of

the

Warm

Springs

area,

the

average

is

slightly

higher

than

that

from

the

basins

south

of

the

divide.

The

significance

attached

to

these

conclusions

depends

largely

upon

the

confidence

that

is

placed

in the

stream-discharge

data

ob-

tained

under

the

circumstances

and

upon

the

accuracy

of

the

deter-

mination

that

the

ground-water

divide

lies

south

of

the

topographic

divide.

Without

doubt,

many

other

elements

affect

the

run-off

from

any

topographic

basin the

elements

that

affect

evaporation,

such

as

soil

and

vegetation;

the

elements

that

affect

transpiration,

such

as

kind

and

distribution

of

vegetation;

the

elements

that

affect

rate

of

absorp-

tion

and

discharge

of

water

by the

rocks.

Few

of

these

can

be

given

quantitative

value.

BOCK

FORMATIONS

The

rocks

that

underlie

the

Warm

Springs

quadrangle

represent

a

wide

variety

of

types.

On

the

basis

of

their

local

features

and

rela-

tions,

supplemented

by

knowledge

of

the

features

and

relations

of

26

THE

WARM

SPRINGS

OF

GEORGIA

similar

rocks

that

are

known

in

northern

Georgia,

they

have

been

separated

into

units,

whose

distribution

is

shown

on

the

geologic

map

(pi.

1).

With

the

exception

of

several

diabase

dikes

that

are

probably

of

Triassic

age

and

several

areas

of

surficial

sand

and

gravel

that

are

probably

Tertiary

or

later,

all

the

rocks

within

the

quadrangle

are

considered

to

be

pre-Cambrian.

These

include

several

large

masses

of

igneous

rocks

that

show

little

evidence

of

change

since

they

were

intruded

and

large

areas

of

sedimentary

and

igneous

rocks

that

have

undergone

considerable

alteration

(metamorphism)

since

they

were

originally

formed.

They

are

a

part

of

the belt

of

crystalline

rocks

that

underlies

much

of

the

Central Upland

of

Georgia

and

the

Pied-

mont

region

of

the

Carolinas

and

Virginia.

PRE-CAMBRIAN

ROCKS

NORTH

OF

TOWAUQA

FAULT

Carolina

gneiss.

The

oldest

rocks

of

this

area

include

biotite

gneiss

and

mica

schist

that

are

here

considered

to

be

the

equivalent

of

rocks

known

in

western

North

Carolina

as

the

Carolina

gneiss.

These

rocks

are

restricted

to

the

part

of

the

quadrangle

that

lies

north

of

the

Towaliga

fault

(pi.

1).

Most

of

them,

particularly

the

fine-grained

biotite

gneiss

and

thinly

laminated

muscovite

schist,

are

considered

to

be

sedimentary

deposits

that

have

been

recrystal-

lized

without

the

addition

of

much

new

material.

The

mapped

unit,

however,

contains

large

areas

of

coarser-grained

and

more

strongly

foliated

rocks,

made

up

of

oligoclase,

biotite,

and

quartz

with

sporadic

muscovite

and

garnet,

that

are

considered

to

be

sedimentary

material

that

has

been

thoroughly

injected

by

granite.

Much

of

the

schist

also

contains

thin

lenses

of

pegmatite

that

conform

to

the

lamination.

Within

the

main body

of

Carolina

gneiss

there

are

numerous

small

lenticular

bodies

of

dark-green

to

black

gneiss

made

up

largely

of

hornblende,

plagioclase,

and

quartz.

The

lamination

of

the

Carolina

gneiss

is

in

large

part

steeply

inclined,

and

the

trends

show

that

it

has

been

involved

in

folding.

The

lenses

of

dark

gneiss

conform

with

the

lamination

of

the

Carolina

gneiss,

and

the

relations

indicate

that

the

dark

gneiss

may

be

the

equivalent

of

the

Roan

gneiss

of

western

North

Carolina,

which

is

inferred

to

be

a

recrystallized

basaltic

rock

intrusive

in

the

Carolina

gneiss.

Snelson

granite.

A

large

area

in

the

northwest

quarter

of

the

Warm

Springs

quadrangle

is

underlain

by

granite

which

is

made

up

largely

of

oligoclase,

microcline,

quartz,

and

biotite

and

which

is

here

called

the

Snelson

granite

because

it

is

well

exposed

near

Snelson's

Crossroads,

*

2Yz

miles

east

of

Harris.

Most

of

the

biotite

flakes

are

arranged

in

rudely

parallel

layers,

so

that

the

rock

has

a

persistent

foliation.

In

contrast

with

the

Carolina

gneiss,

the

foliation

shows

small

folds

and

minute

plications.

Like

the

gneiss,

however,

the

Snelson

granite

is

cut

by

numerous

pegmatite

dikes,

some

of

which

contain

tourmaline.

BOOK

FORMATIONS

27

Regional

and

local

relations

indicate

that

the

granite

is

intrusive

into

the

gneiss.

The

contact

between

these

rocks

is

not

sharp

but

broadly

gradational,

and

near

it

the

gneiss

contains numerous

lenses

of

granitic

material

that

have

been

injected

along

the

planes

of

lamination.

The

area

within

which

the

Carolina

gneiss,

Snelson

granite,

and

Roan

gneiss

are

included

ends

southward

against

a

narrow

belt

of

sheared

rock,

largely

Carolina

gneiss,

which

has

been

traced

for

many

miles

through

western

Georgia

and

is

known

as

the

Towaliga

fault

zone.

Without

doubt

it

is

a

major

structural

feature,

for

the

rocks

that

lie

north

of

it

are

not

known

south

of

it,

and

conversely

those

that

lie

south

of

it

are

not

known

north

of

it.

PBE-CAMBBIAN

BOCKS

SOUTH

tfF

TOWALIGA

FAULT

Sparks

schist.

The

oldest

rocks

in

the

area

south

of

the

Towaliga

fault

are

confined

to

a

belt

3

to

5

miles

wide

that

extends

eastward

across

the

quadrangle

between

Pine

and

Oak

Mountains.

The

belt

includes

several

varieties

of

mica

schist,

biotite

gneiss,

and

quartzite,

which

are

so

interlayered

as

not

to

be

separable

in

areal

mapping.

These

rocks

are

here

called

the

Sparks

schist,

because

they

are

well

exposed

along

Sparks

Creek,

which

flows

southward

near

the

western

border

of

the

quadrangle.

The

schist

is

a

medium-grained

rock

made

up

largely

of

muscovite,

biotite,

quartz,

and

feldspar.

The

gneiss

is

made

up

of

feldspar,

biotite,

and

minor

quartz

and

garnet

and ranges

from

fine-

to

coarse-grained.

There

are

thin

beds

of

quartzite

in

both

the

schist

and

the

gneiss.

In

contrast

with

the

overlying

Hollis

quartzite,

however,

they

contain

more

feldspar

and

grade

into

feld-

spathic

quartz-mica

schist.

The

Sparks

schist

is

considered

to

be

a

highly

metamorphosed

sedimentary

deposit

into

which considerable

granitic

material

has

been

injected.

Hollis

quartzite.

Overlying

the

Sparks

schist

is

the

Hollis

quartzite,

a

distinctive,

persistent

unit

that

is

important

in

the

problem

of

both

warm

and

cold

spring

waters

in this

region.

The name

'was

first

applied

by

Adams

4

to

quartzites

that

crop

out

near

Hollis,

on

the

Central

of

Georgia

Railway,

6

miles

southeast

of

Opelika,

Ala.

Field

work

during

recent

years

has

shown

that

the

quartzite

may

be

readily

traced

from

the

vicinity

of

Notasulga,

Ala.,

northeastward

about

100

miles

to

Barnesville,

Ga.

It

is

well

exposed

in

the

"Warm

Springs

quadrangle,

where

it

sustains

the

persistent

ridges

of

Pine

Mountain

and

Oak

Mountain.

All

the

warm

springs

of

the

region

and

appar-

ently

most

of

the

larger

cold

springs

issue

along

or

near

the

upper

layer

of

quartzite,

where

it

dips

under

the

overlying

Manchester

schist.

At

several

localities

in

Alabama

a

thick

layer

of

dolomite,

the

'

Adams,

G.

D.,

Geology

of

Alabama:

Alabama

Geol.

Survey

Special

Kept.

14,

p.

36,1936;

The

significance

of

the

quartzite

of

Pine

Mountain

in

the

crystallines

of

west-central

Georgia:

Jour.

Geology,

vol,

38,

pp.

271-279,1930;

General

geology

of

the

crystallines

of

Alabama:

Jour.

Geology,

vol.

41,

pp.

169-171,1933.

28

THE

WARM

SPRINGS

OF

(GEORGIA

Chewacla

marble,

is

present

near

the

Hollis

quartzite,

but

the

sequence-

is

not

clear.

The

Chewacla

marble

is

not

known

in

western

Georgia^

The

features

of

the

Hollis

quartzite

are

well

shown

in

the

Warm

Springs

quadrangle

at

numerous

natural

exposures

on

the

slopes

of

Pine

and

Oak

Mountains,

especially

in

the

gorges

cut

by

the

Flint

River

and

in

numerous

road

and

railway

cuts.

Measurements

of

its

thickness

on

Pine

Mountain

range

from

275

feet

at

Dunn's

Gap

to

nearly

800

feet

along

the

Flint

River

where

it

passes

through

the-

Cove.

Along

Oak

Mountain

the

thickness

appears

rarely

to

exceed

300

feet.

Throughout

this

region

the

quartzite

is

very

pure

silica_

Muscovite

commonly

occurs

in

small

amounts;

very

rarely,

green

chromium

mica

is

present.

Albite

feldspar

occurs

at

a

few

places.

Sparse

rounded

grains

of

zircon

arranged

in

parallel

layers

tend

to

confirm

the

sedimentary

origin

of

the

quartzite.

In

this

region

the-

upper

and

lower

100

feet

are

generally

thin-bedded

and

the

middle*

part

is

thick-bedded.

Artificial

exposures

of

the

upper

part

commonly

show

layers

of

rather

pure

silica,

an

eighth

of

an

inch

to

an

inch

thick,,

separated

by

thin persistent

layers

of

mica;

such

material

where-

weathered

is

commonly

flexible,

and

the

name

"itacolumite"

has

been

applied

to

it.

By

contrast,

the

beds

of

the

middle

part

in

numerous

natural

exposures

are

2

to

10

feet

thick

and

are

broken

only

by

vertical

joints.

^The

examination

of

numerous

polished

and

thin

sections

of

the

quartzite

failed

to

reveal

evidence

of

the

size

and

shape

of

the-

original

grains

of

quartz,

of

which

it

was

doubtless

once

composed.

At

present

the

grains

are largest in

the

thick-bedded

material

and

smallest

in

the

thin-bedded

material.

In

the

thick-bedded

rock

most

of

the

volume

is

made

up

of

grains

5

to

10

millimeters

(0.2

to

0.4

inch>

long;

in the

thin-bedded

rock

few

grains

exceed

1

millimeter.

In.

shape

the

grains

are

irregularly

elongated

parallel

to

the

bedding,

but

their

outlines

are

also

minutely irregular

or

crenulate

and

inter-

locking.

Most

of

the

grains

show

undulatory

extinction

under

the

microscope.

The plates

of

muscovite extend

from

one

grain

of

quartz

into

another

adjoining.

In

contrast

to

most

unmetamorphosed

sandstones,

this

quartzite-

would

seem

to

be

a

poor

aquifer.

Tests

of

numerous

specimens,

however,

including

one

from

the

bottom

of

the

90-foot

Norris

well

recently

dug

on

Pine

Mountain,

show

that

colored

liquids

penetrate-

it

rapidly.

It

is

therefore

believed

that

the

upper

and

lower

thin-

bedded

parts,

each

100

feet

or

more

thick,

are

relatively

permeable

and

act

as

fair

water

carriers,

in

contrast

with

the

middle,

more-

massive

part,

which

seems

to

be

relatively

impervious.

On

the

top

and

along

the

upper

slopes

of

Pine

Mountain

the

quartzite

weathers-

to

loosely

coherent

sand.

The

Butts

well,

on

the

top

of

Pine

Moun-

tain,

was

dug

to

a

depth

of

85

feet

in

the

middle

part

of

the

quartzite-

by

the

use

of

pick

and

shovel.

By

contrast,

blasting

was

necessary-

BOOK

FORMATIONS

29

in

digging

the

Norris

well

to

a depth

of

90

feet

in

the

quartzite

about

300

feet

below

the

top.

Where

the

Hollis

quartzite

is

thin-bedded,

it

seems

quite

clear

that

the

laminations

represent

the

stratification

of

the

original

sandstone.

In

the

thick-bedded

portions,

however,

local

discordances

of

the

part-

ing surfaces

raise

doubt

concerning

the

accuracy

with

which

they

show

the

attitude

of

the

entire

sheet.

The

field

work

shows

that

in

most

places

the

parting

surfaces

of

the

upper and

lower

thin-bedded

quartz-

ite

reveal

the

structure

of

the

unit.

Manchester

schist. A

thick

mass

of

mica

schist

and biotite

gneiss,

here

called

the

Manchester

schist,

overlies

the

Hollis

quartzite.

It

is

named

for

the

largest

town

in

this

quadrangle.

The

formation

is

exposed

in

two

belts

that

extend

generally

northeast,

one of

which

lies

north

of

Pine

Mountain

and

the

other

south

of

Oak

Mountain.

There

is

considerable

resemblance

between

the

Manchester

schist,

above

the

Hollis

quartzite,

and

the

Sparks

schist,

below

the

quartzite,

and

it

is

thought

that

both

were

originally

sedimentary

deposits

that

have

undergone similar

changes.

The

mica

schist

is

largely

musco-

vite,

but

variable

amounts

of

quartz,

biotite,

and

oligoclase

are

present.

Accessory

minerals

include

garnet

and

apatite;

more

rarely

hypersthene

and

kyanite.

In

the

vicinity

of

Warm

Springs

the

schist

contains

enough

graphite

to

mark

paper.

Most

of

the

gneissic

ma-

terial

is

present

as

thin

layers,

largely

a

quarter

of

an

inch

to

several

inches

thick.

The

rock contains

considerable

plagioclase

(oligoclase

to

andesine),

some

of

which

forms

large

augenlike

crystals,

quartz,

biotite,

muscovite,

and

garnet.

Accessory

minerals

include

zircon,

apatite,

orthoclase,

tourmaline,

and

rutile;

more

rare

are

chlorite

and

calcite.

At

about

850

feet

above

the

base

of

the

Manchester

schists,

both

south

of

Oak

Mountain

and

locally

north

of

Pine

Mountain, there

is

a

persistent

bed

of

quartzite

that

ranges from

50

to

300

feet

in

thick-

ness.

It

closely

resembles

the

Hollis

quartzite.

Woodland

gneiss.

The area

south

of

the

Towaliga

fault

contains

bodies

of

pre-Cambrian

igneous

rocks

of

two

varieties an

earlier,

here

called

the

Woodland

gneiss,

and

a

later,

here

called

the

Cun-

ningham

granite.

The

earlier rock

is confined

to

the

belt

that

lies

between

Pine

and

Oak

Mountains;

the

later

rock

is

found

both

in

this

belt

and south

of

Oak

Mountain.

The

Woodland

gneiss

is

named

for

the

town

of

Woodland,

in

the

southeast

corner

of

the

quadrangle.

It

is

largely

a

coarse-grained

biotite

augen

gneiss,

so

called

on

account

of

the

coarse

lenticular

orthoclase

crystals

that

are

rather

uniformly

distributed

through

a

medium-grained

mass

of

orthoclase,

quartz,

and biotite.

Muscovite

and

garnet

are

common,

and

apatite

and

zircon

are

sparingly

present.

The

Woodland

gneiss

persistently

underlies

the

basal

bed

of

the

30

THE

WARM

SPRINGS

OF

GEORGIA

Hollis

quartzite

in

this

quadrangle.

The

100

feet

or

more

of

gneiss

that

immediately

underlies

the

quartzite

is

thinly

laminated,

locally

almost

schistose;

progressively

lower

or

deeper

in

the

mass

the

lami-

nation

is

more

widely

spaced,

and

the

rock

assumes

the

common

gneissic

texture.

As

this

gneiss

is

the

most

completely

metamor-

phosed

of

the

igneous

rocks

of

this

region,

it

is

assumed

to

be

the

oldest.

Cunningham

granite.

The

Cunningham

granite

forms

one

large

and

several

small

bodies

in

the

south

half

of

the

quadrangle.

In

contrast

with

the

other

igneous

and

metamorphic

rocks

of

the

region,

it

is

dark

in

color,

and

the

boundaries

can

be

traced

with

confidence.

Commonly

it

is

a massive

coarse-grained

rock

made

up

of

orthoclase,

andesine,

quartz,

biotite,

garnet,

augite,

and

hypersthene,

named

in

the

order

of

their

abundance;

apatite,

zircon,

and

piedmontite

are

accessory

minerals.

In

a

few

places

the

rock

is

gneissic.

The

boundaries

locally

cut

across

the

lamination

of

the

Woodland

gneiss,

and

the

granite

is

believed

to

be

intrusive

in

this

rock.

It

is

named

for

Cunningham

Crossroads,

southeast

of

Manchester,

where

the

central

part

of

the largest

mass

of

the

rock

is

exposed.

TBIASSIC

IGNEOUS

BOOKS

Several

diabase

dikes

are

present in

the

quadrangle.

They

are

interesting

because

they

are

uncommonly

long

for

their

width and

because

they

cut

across

all

the

other

rocks

of

the

region.

The

longest

of

these,

the

Talbotton

dike,

which

crosses

Oak

Mountain

4,000

feet

west

of

Woodland,

extends

for

35

miles,

but

its

maximum

width

is

only

155

feet.

The

average

width

of

the

other

dikes

is

about

30

feet.

The

dike

rock

is

largely

made

up

of

laths

of

labradorite

with

augite;

quartz,

biotite,

and

iron

oxides

are

sparingly

present;

olivine

is

not

known

in

the

dikes

of

this

area.

Such

dikes

have

been

found

over

a

large

area

in

the

Piedmont

region.

They

are

generally

assigned

to

the

Triassic.

TERTIARY

(?)

AND LATER

SEDIMENTARY

ROCKS

The topographic

map

shows

that

the

high

parts

of

Pine

Mountain

in

this

region

are

nearly

flat.

These

flat

surfaces

range

in

altitude

from

about

1,250

feet

to

1,395

feet

on

Dowdell

Knob,

which

is

the

highest

point

in

the

quadrangle.

They

appear

to

be

remnants

of

a

flat

surface

that

was

once

extensive

in

this

region

but

is

now

preserved

only

where

it

is

underlain

by

resistant

Hollis

quartzite.

Most

of

these

flat

remnants

show

thin

sporadic

patches

of

subangular

to

round

quartzite

pebbles,

mainly

from

1

to

3

inches

in

diameter.

The

pebbles

do

not

form

a

continuous

layer

but

are

embedded

in

the

layer

of

residual

sandy

soil

1

to

2

feet

thick

derived

from

the

Hollis

quartzite.

Until

the

geologic

features

of

a

large

region

in

central

Georgia

are

further

studied

the

correlation

and

age

of

these

gravel

deposits

can

STRUCTURAL

FEATURES

31

only

be

inferred.

For

the

present

it

seems

that

they

were

laid

down

by

coastal

streams

at

some

stage

in

the Tertiary

period.

At

four

localities

on

the

north,

east,

and

south

borders

of

the

wide

lobe

of

Pine

Mountain

south

of

Warm

Springs

there

are

patches

of

unconsolidated

sand

and

clay

that

rest

on

deeply

weathered

crystalline

rocks,

mostly

Manchester

schist.

Their

outcrops

range

in

altitude

from

850

to

980

feet,

and

the

thickest

appears

to

be

about

90

feet

thick.

Particular

interest

is

attached

to them

because

at

least

one,

that

near

Mount

Hope

Church,

contains

masses

of

bauxite

and

kaolin,

several

of

which

have

been

explored

and

have

yielded a

small

production.

The

age

of

these

deposits

is

obscure,

but

they

are

younger

than

the

gravel

on

Pine

Mountain.

STRUCTURAL FEATURES

'

All

the

rocks

of

this

area,

except

the

diabase

dikes

and

unconsolidated

materials,

are

metamorphic that

is,

they

have

been

thoroughly

re-

crystallized

since

their

original

formation.

The

rocks

that

were

once

sediments

now

include

mica

schist,

quartzite,

and

biotite

gneiss;

igneous

rocks

are represented

by granite

gneiss,

augen

gneiss,

and

hornblende

gneiss.

Furthermore,

most

of

the

rocks, as

a

result

of

these

changes,

have

assumed

a

strong

foliation.

Although

the

folia-

tion

of

the

sedimentary

rocks

now

lies

in

diverse

attitudes,

it

is

almost

certainly

closely

coincident

with

the

original

bedding.

This

is

par-

ticularly

evident

in

the

Hollis

quartzite,

where

bedding

is

indicated

by

layers

of

different

texture

and

foliation

is

indicated

by

alinement

of

mica

scales.

The

outstanding

fault

is

that

known

as

the

Towaliga

fault,

which

crosses

the

area

north

of

Warm

Springs,

extending

in

a

northeasterly

direction

(pis.

1

and

2).

In

places

the

evidence

is

good

that

the

fault

plane

dips

about

50°

NW.,

but

as

the

Carolina

gneiss,

which

lies

north

of

the

fault,

is

the

oldest

rock

in

the

region,

and

the

rocks

of

the

Wa-

coochee

belt,

which

lie

south

of

the

fault,

appear

to

be

much

younger,

it

follows

that

the

region

north

of

the fault

has

been

raised,

and

the

fault

must

be

regarded

as

an

overthrust.

It

also

follows

from

this

interpretation

that

the

Hollis

quartzite

dipping

northwest

from

Pine

Mountain must

be

cut

off

in

depth

by

this

fault.

These

relations

are

used

to

explain

the

probable

course

of

the

water

that

appears

at

Warm

Springs.

The

diabase

dikes

fill

fractures,

but

these

do

not

appear

to

be

faults.

A

small

fault

displaces

one

of

the

dikes,

and

two

other

faults

are

indi-

cated

on

the

south

side

of

Pine

Mountain

near

Nebula.

Without

doubt

there

are

many

other

faults and

fractures

in

this

region,

but

they

do

not

appear

to

be

extensive

enough

or

great

enough

to

displace

noticeably

the

boundaries

of

the

formations

that

have

been

mapped.

Several

large

anticlinal

folds

and numerous

small

ones

are

revealed

by

the

mapping

of

the

Hollis

quartzite.

The

largest

is

that

of

which

32

THE

WARM

SPRINGS

OF

GEORGIA

the

outcrops

on

Pine

Mountain

form

the

north

limb

and

those

on

Oak

Mountain

the

south

limb.

The

Cove

is

carved

out

of

the

center

of

a

nearly

circular

dome,

so

that

the

Hollis

quartzite

forms

the

limit-

ing

rim.

Numerous

small

folds,

both

anticlines

and

synclines,

are

revealed

by

outcrops

of

the

Hollis

quartzite

on

the

crest

of

Pine

Mountain

south

of

Warm

Springs

and

near

the

Flint

River

and

by

outcrops

of

the

Manchester

schist.

The

small

anticline

shown

by

outcrops

of

Hollis

quartzite

around

the

hill

occupied

by the

Warm

Springs

Foundation

seems

to

be

a

factor

in

localizing

the

outlet

of

Warm

Springs

(pi.

3).

Most

of

the

minor

folds

of

the

region

are

indicated

on

plate

3.

SOURCE

OF

THE

WARM

SPRINGS

WATER

I

The

data

from

several

phases

of

this

investigation

tend

to

show

that

the

water

issuing

from

the

Warm

Springs

is

that

which

falls

as

rain

on

the

high

parts

of

Pine

Mountain

within

several

miles

of

the

springs.

These

data

may

be

summarized

briefly

as

follows:

1.

The

surface

run-off

from

the

drainage

basins

north

of

the

Pine

Mountain

divide

is

less

per

unit

of

area

than

that

of

the

basins

south

of

the

divide,

and

this

difference

is

about

made

up by

the

combined

dis-

charge

of

Warm

Springs

and

Cold

Springs

(pis.

7,8).

2.

The

run-off

per

unit

of

area

of

the

basins

that

drain

southward

from

Pine

Mountain

is

rather

uniform;

by

contrast,

the

basins

that

drain

northward

show

great

variations

in

run-off,

and

there

is

a

notable

deficiency

in

the

basins

that

lie

within

3

miles

south

and

southwest

of

Warm

Springs.

The

two

fairly

large

basins

that

lie

south

of

Warm

Springs

and

Cold

Springs yield

no run-off

except

during

storms.

3.

The

fluctuations

in

discharge

of

Warm

Springs

have

a

definite

re-

semblance

to

the

fluctuations

in

rainfall

as

shown

by

the

gage

on

the

top

of

Pine

Mountain,

3

miles

south,

but

the

highs

and

lows

of

spring

discharge

lag

6

or

7

weeks

behind

the

highs

and

lows

of

rainfall

(pi.

4).

The

water

level in

a

well

in

the

lower

part

of

the

Hollis

quartzite

near

the

rain

gage

on

Pine

Mountain

shows

similar

highs

and

lows

that

also

lag

2

to

5

weeks

behind

those

of

rainfall

(pL

4).

This

relation

is

one

that

would

be

expected

if

the

well

penetrates

an

aquifer

that

is

connected

with

the

conduit

by

which

the

water

of

Warm

Springs

rises

to

the

surface.

4.

The

water

of

Warm

Springs

is

relatively

low

in

dissolved

solids;

it

does

not

contain

boron,

and,

so

far

as

shown

by

the

analyses,

it

does

not

contain

any

dissolved

ingredients

that

suggest

a

deep

igneous

origin.

5.

The

gases

dissolved

in

the

water

of

Warm

Springs

are

those

found

in the

air,

and

they

occur

in

about

the

same

proportion

that

they

occur

in

the

air,

except

that

the

percentage

of

nitrogen

is

slightly

higher

and

the

percentage

of

oxygen

slightly

lower.

Carbon

dioxide,

if

SOURCES

OF

THE

WARM

SPRINGS

;WATER

present

in

large

quantities,

might indicate

a

deep

igneous.originybufi

this

gas

occurs

in

the

water

of

Warm

Springs

in

<)nly

moderate

amounts,'

such

as

would

normally

be

dissolved

by

water

of

surface

origin

Hfrom

the

air

and

soil in

fact

it

is

even

less

in

Warm

Springs

than

in

Cold

Spring.

The

structure

of

the

rocks

in

the

vi-

cinity

of

Warm

Springs

is

shown

in

the

geologic

section

given

in

figure

1.

The

structure

at

considerable

depths

of

course

could

not

be

observed,

but

it

is

inferred

from

the

structure

as

re-

vealed

at

the

surface.

The

arrows

in

the

figure

show

the

probable

path

of

the

water

discharged

by

Warm

Springs.

Starting

as

rain

on

parts

of

Pine

Moun-

tain

where

the

dense

middle

member

of

the

Hollis

quartzite

has

been

re-

moved

by

erosion

or

is

sufficiently

fractured

to

permit

some

downward

percolation,

the

water

percolates

into

the

permeable

basal

beds

of

the

Hollis

quartzite

and

thence

northward

through

these

beds

to

great

depths,

where

it

becomes

heated

by

the

nat-

ural

heat

of

the

rocks.

From

the

struc-

ture

of

the

rocks

and

the

thermal

gradient

(p.

34)

it

is

concluded

that

the

water

percolates

northward

nearly

to

the

Towaliga

fault.

Near

the

fault

it

probably

percolates

upward,

through

fractures

in

the

dense

middle

member

of

the

Hollis

quartzite,

into

the

upper

permeable beds

of

this

formation.

Thence

it

is

forced

upward

by

artesian

pressure

through

these

permeable

beds,

in

which

it

is

confined

by

the

nearly

impermeable

middle

member

below

and by

the

nearly

impermeable

Manchester

schist

above,

and

even-

tually

it

reaches

the

surface

at

Warm

Springs.

In

its

upward

course,

before

it

reaches

the

surface,

the

;

water

flows

mainly

through

one

or

more

natural

conduits,

which

may

have

been

pro-

duced largely

by

the

solvent

action

of

the

water.

34

THE

WjSbBM

SPRINGS.OF

GEORGIA

The

remaining

warm

springs

of

the

region,

Parkman,

Brown's,

Thundering,

Barker,

LAfsey,

and

Taylor,

rise

either

from

Manchester

schist

within

a

few

hundred

feet

above

the

top

of

the

Hollis

quartzite

or from

the

thin

layers

of

local

alluvium

that

overlies

the

schist.

As

shown

in

plate

2,

the

areal

distribution

of

the

warm

springs

in

the

Wacoochee

belt

of

rocks

clearly

indicates

a

relation

to

these rocks,

particularly

to

the

Hollis

quartzite,

but

the

observations

which

would

be

needed

to

indicate

the

course

of

the

water

that

now

issues

at

these

warm

springs

have

not

been

made.

The

water

may

either

have

entered

the

upper

layers

of

the

Hollis

quartzite

and

descended

several

hundred

feet

below

the

surface

before

encountering

fractures

through

which

it

could

rise

to

the

surface,

or,

conceivably,

it

may

have

entered

the

lower

layers

of

the

Hollis

quartzite

and,

after

descending

below

the

surface,

encountered

fractures

that

crossed

the

entire

thickness

of

quartzite

as

well

as

the

overlying

Manchester

schist.

Without

doubt,

the

Towaliga

fault

persists

to

great

depth.

If

it

were

assumed

that

it

cuts

deep

reservoirs

of

water,

possibly

of

volcanic

origin,

one

would

expect

these

waters

to

rise

as

warm

springs

along

the

fault.

Most

of

the

warm

springs,

however,

appear

at

the

surface

from

3

to

8

miles

distant

from

the

fault.

It

is

believed,

therefore,

that

the

fault

plays

no

direct

part

in

localizing

the

distribution

of

the

springs.

SOURCE

OF

THE

HEAT

OF

WARM

SPRINGS

WATER

The

diagram

that

is

presented

as

figure

1

to

show

the

source

and

path

of

the

water

that

issues

at

Warm

Springs

indicates

also

the

prob-

able

source

of

the

heat.

There

can

be

little

doubt

that

the

Hollis

quartzite

extends

northward

from

the

springs

under

the

Manchester

schist

and

ends

in

depth

against

the

Towaliga

fault.

The

dip

of

the

quartzite

as

it

passes

downward

under

the

schist

and

the

dips

shown

in

the

schist

indicate

that

the

quartzite

attains

a

depth

of

about

3,800

feet

below

the

local

surface.

As

no

record

of

thermal

gradients

in

the

crystalline

rocks

of

Georgia

was

available,

accurate

measurements

of

temperature

were

made

at

100-foot

intervals

in

two

wells

during

this

investigation.

There

are

numerous

wells

in

the

crystalline

rocks

as

much

as

800

feet

deep

from

which

water

is

pumped

for

use

as

local

domestic

supplies.

The

wells

chosen

for

measurement

were

one

\%

miles

west

of

Griffin,

Ga.,

757

feet

deep,

and

another

at

Youngs

Mill,

6

miles

northeast

of

LaGrange,

618

feet

deep,

respectively

35

miles

northeast

and

23

miles

northwest

of

Warm

Springs.

Neither

well

had

been

used

for

several

years

before

the

temperature

was

measured.

Both

wells

were

drilled

in

granite

gneiss,

which

appears

to be

included

in

the

Carolina

gneiss

of

this

region.

Only

the

temperatures

below a

depth

of

300

feet

were

used

in

calculating

the

thermal

gradient.

In

the

Griffin

well

the

temperature

increased

0.95°

F.

for

each

100

feet

in

depth,

and

in the

SOURCE

OF

THE

COLD

SPRING

WATER

35

LaGrange

well,

1.20°

F.

These

gradients

indicate

a

temperature

of

99.2°

F.

at

a

depth

of

3,800

feet

at

the

Griffin

well

and

of

89.5°

F.

at

the

LaGrange

well.

It

appears

that

a

thermal

gradient

such

as

that

found

at

the

LaGrange

well

is

sufficient

to

heat

the

water

so

that

it

could

be

delivered

at

the

surface

at

a

temperature

of

88°

F.,

after

allowance

is

made

for

the

loss

of

heat

that

must

occur

during

the

up-

ward

movement

of

the

water.

This

is

the

temperature

of

the

Warm

Springs

water.

The

geologic

and

thermal

data

indicate,

therefore,

that

water

enter-

ing

the

ground

on

Pine

Mountain

at

a

temperature

of

62°

F.

can

be

carried

in

the

Hollis

quartzite

to

a

depth

of

about

3,800

feet

and

re-

turned

to

the

surface

at

a

temperature

of

88°

F.

SOURCE

OF

THE

COLD

SPRING

WATER

Even

the

casual observer

is

impressed

by

the

fact

that

the largest

cold

spring

of

this

region

(Cold

Spring)

appears

at

the

surface

scarcely

a

mile

from

the

largest

warm

spring

(Warm

Springs),

and

it

is

natural

to

wonder

whether

they may

be

related.

During

the

period

of

study,

the

discharge

of

Cold

Spring

Branch,

as

noted

from

32

measurements,

ranged

from

1,282

to

1,822

gallons

a

minute

and

the

average

was

1,546

gallons.

This

is

essentially

the

discharge

of

the

four

cold

springs.

Although

the area

of

the

surface

drainage

basin

of

Cold

Spring

Branch

is

507

acres,

there

is

no

run-off

from

that

part

of

the

basin

above

Cold

Spring.

As

the

average

dis-

charge

of

Cold

Spring

Branch

represents

all

the

water

that

would

fall

as

rain

on

667

acres

at

theTate

of

45

inches

a

year,

it

is

clear

that

Cold

Spring

must

receive

water

from

a

larger area

than

the

surface

basin

that

lies

above

it.

Both

the

chemical

character

and the

temperature

of

the

water

indicate

that

it

has

not

penetrated

far

below

the

surface

of

the

ground.

A

study

of

the

rainfall

and

run-off

from

the

Mill

Creek

Basin,

5

miles

west

of

Warm

Springs,

indicates

that

33

percent

of

the

rainfall

is

represented

by the

run-off

of

the

stream,

the

remaining

67

percent

being

lost

by

evaporation,

transpiration,

percolation

out

of

the

basin,

and

other

minor

processes.

From

this

study

it

would

appear

that

these

cold

springs

are

discharging

the

water

that

is

absorbed

as

rain

in

the

shallow

surficial

zone

of

an

area

that

must

range from

1,500

to

2,000

acres,

south

and

southwest

of

the

springs.

This calculation

indicates,

therefore,

that

the

water

discharged

by

the

cold

springs

must

represent

the

rainfall,on

several

Jiearby-surface

basins

taut

that

much«

of

the

water,

instead

of

following

the

surface

drains,

enters

the

permeable

upper

200

feet

of

Hollis

quartzite,

follows

this

zone

laterally

eastward

below

the

Manchester

schist,

and

is

delivered

as

cold

springs

at

the

lowest

surface

outcrop

of

this

zone.

The

existence

of

the

largest

cold

spring

relatively

near

the

largest

warm

spring

is

probably

to

be

explained

by

the

areal

extent

of

the

36

THE

WABM

SPRINGS,OF

GEORGIA

outcrop-

and

the

structure

of

the

Hollis

qdartz&e.

It

has

been

stated

earlier

that

the

distribution

of

the

known

warm

springs

of

Georgia

seems

to

be

and

therefore

controlled

by

the

belt

of

Hollis'

quartzite.

Plate

2

.shows

the

approximate

areal

extent

of

the

quartz*

ite

outcrops.

Where

the

outcrop

is

narrow

the quartzite

dips

steeply;

where

it

is

broad

the

quartzite

is

either

closely

folded,

as

near

the

Flint

River,

or

reveals

broad

gentle

folds,

as

south

of

Warm

Springs.

The

great

lobe

of

quartzite

that

forms

Pine

Mountain

south

of

Warm

Springs

is

the

largest

outcropping

body

of

the

quartzite

and,

although

gently

folded,

it

dips

generally

north

and

northeast.

Such

an

area

offers

the

best

opportunity

in

the

region

for

the

upper

part

of

the

Hollis

quartzite

to

absorb

rainfall.

The

general

trend

of

movement

and

point

of

discharge

of

such

absorbed

water

would

be

governed

by

the

structure

of

the

beds

and

the

distribution

of

ravines.

It

seems

reasonable,

therefore,

that

the

largest

cold

spring

of

the

region

should

be

found

adjacent

to

the

largest

outcrop

of

gently

dipping

quartzite,

According

to

the

interpretation

of

the

source

and

underground

move-

ment

of

the

water

of

Warm

Springs,

offered

here,

it

is

reasonable

that

this

water,

too,

should

be

found

adjacent

to

the

largest

outcrop

of

Hollis

quartzite.

Both

springs

apparently

derive

their

water

from

rain

falling

on

the

surface.

The

difference

in

temperature

is

due

to

the

difference

in

the

depth

to

which

the

water

percolates

in

the

earth

before

reappearing

at

the

surface.

MEASURES

FOB

IMPROVING

THE

WARM

SPRINGS

It

was

the

hope

of

the

officials

of

the

Georgia

Warm

Springs

Foundation

that,

as

the

result

of

this

investigation,

ways

might

be

found

by

which

the

temperature

of

the

water and

perhaps

the

dis-

charge,

might

be

increased.

The

investigation

shows

that

about

two-thirds

of

the

total

supply

of

warm

water

in

the

area,

or

about

.550

gallons

a

minute,

has

an

observed

temperature

ranging

only

between

87.7°

and

88.2°

F.,

and

that

it

issues

from

a

fractured

zone

in

the

quartzite

scarcely

25

feet

wide.

The

other

one-third

of

the

water

issues

from

numerous

outlets

in

alluvium,

within

250

feet

east

or

west

of

the

main

source,

and

with

temperatures

as

much

as

9°

lower

than

that

of

the

main

source.

Doubtless

all

sources of

warm

water

should be

controlled

sooner

or

later,

but

at

present

the

warmest

two-thirds

should be

segregated

from

the

sources

of

cooler

water.

It

seems

that

the

minor

sources

of

water

that

issues

from

local

alluvium

may

be

regarded

as

leakage from

a

central

or

main

conduit.

It

would

therefore

be

advisable

to

enclose

the

minor

sources

in

walls

of

impermeable

material,

making

a

tight

seal

with.the

bedrock

and

rising

above

the

present outlets

so

as

to

form

pools

in

which

water

levels

would

lie

several

feet

above

the

present

outlets.

Back

pressure

MEASURES

FOR

IMPROVING

THE

WARM

SPRINGS

37

would

thus

be

created,

which

would

tend

to

force

the

water

to

rise

in

the

central

conduit,

probably

at

the

present

temperature

of

that

portion.

The

question

has

been

raised

whether

it

would be

possible

by

drilling

to

intercept

the

main

or

central

conduit

at

depth

and

permit

the

water

to

rise

directly

to

the

surface,

probably

with

less

loss

of

heat

than

takes

place

in

the

natural

conduit.

All

that

can

be

learned

of

the

local

geology

and

inferred

concerning

the

path

of

the

rising

water

indicates

that

the

chance

of

intercepting

the

natural

conduit

at

a

depth,

say,

of

500

feet,

by

one

or

a

few

vertical

holes,

is

very

small.

For

the

increase

in

temperature

that

might

be

expected,

it

seems

that

the

expenditure

would

not

be

warranted.

INDEX

Abstract__________

Acknowledgments

for

aid .

Agriculture,

development

of.

Page

1

2

3

21

Analyses

'of

spring

stream,

add

well

waters...

17-26

Barker

Spring,

analysis

of

water

of______

17

discharge

and

temperature

of_.

____

10

geologic

relations

of____________

10,34

location

of_________________

10,19

Black

Sulphur

Spring,

analysis

of

water

of_

17

location

and

general

features

of______

14

Blue

Spring,

analysis

of

water

of

_______

17

chemical

character

of

water

of.. ____

15

discharge

and

temperature

of.______

13

location

of____.____._....___

13,19

Brown's

Spring,

analysis

of

water

of

_____

17

discharge

and

temperature

of__..___

4,10

geologic

relations

of.____________

34

location

of

_________________

10,19

Carolina

gneiss,

general

features

of______

26

geologic

relations

pf,

to

springs._____

14

structural

relations

of__________

31

thermal

gradient

in

well

drilled

in.

___

34

Cascade

Branch,

analysis

of

water

of....

__

18

Central

Upland,

relations

of

_________

3

Chalybeate,

springs

at,

chemical

character

of

water

of_.....______...

1&-14,15

springs

at,

discharge

and

temperature

of..

14

Chalybeate

Spring

(at

White

Sulphur

Springs),

analysis

of

water

of__

17

location

of__________________

14,19

Chalybeate

Spring

Nos.

1-3,

analysis

of

water

of....... ......................

17

Chalybeate

Spring

No.

4,

analysis

of

water

of.

18

Chattahoocb.ee

River,

relation

of

streams

of

area

to_______________

3

Chemical

character

of

the

waters,

data

on__

15-20

Cold

Spring, analyses

of

gases

from____..

21

analysis

of

water

of____________

17

discharge

of,

relation

of,

to

rainfall__

12,

pi.

5

general

features

of..____________

11-12

location

of.._...__..-.---_____...

11,19

source

of

water

of_____________

35-36

temperature

of____________

__

12

Cold

Spring

Branch,

discharge

of._.__._

13,25

discharge

of,

relation

of,

to

rainfall____

35

Cold

springs, analyses

of

waters

of._____

17-18

general

features

of...___....__.__

11-14

summary

of._..______.._____

14

Cold

waters,

chemical

character

of_____

15-16

Columbus,

Qa.,

rainfall

at__________

22

Cove,

features

of

the______________

3,32

Cunningham

granite,

general

features

of___

30

Dikes, diabase,

general

features

of.-----------

30

Dowdell

Knob,

features

of_________..

3,30

Discharge~of.stream&,and-sprkigs,..__.__

4,

6-9,23-25,

pis.

4,7,8

program

of

measurements

of..____...

21

See

also

individual

springs.

Page

Discharge

of

Warm

Springs,

relation

of,

to

rainfall

and

ground-water

level.

23,

pi.

4

Faults

in

the

area .

31

Field

studlte^durmW

of..

2

Flint

River,

relation

of

streams

of

area

to

3

Folds

in

the

area. .------ . - -

31-32

Fuller

well,

analysis

of

water

oL

18

Gases

in

the

spring

waters,

occurrence

and

analyses

of.

21

Geology

of

the

area_._ ...

25-32,

pis.

1,

2

Georgia

Warm

Springs

Foundation,

property

of......

4

property

of,

proposed

measures

for

im-

provement

of

springs

on....

36-37

Gill

Spring,

analysis

of

water

of

18

location

of

20

Greenville

Plateau,

erosion

and

gullying

of...

3

general

features

of...-

2-3

Griffin,

Ga.,

thermal

gradient

in

well

near....

34

Ground-water

level,

fluctuations

of,

in

wells.

23,

pi.

6

relation

of

discharge

of

Warm

Springs

to

rainfall

and . .

23,

pi.

4

Heat

of

Warm

Springs

water,

source

of.

34-35

Hollis

quartzite,

general

features

of

27-29

relation

of

springs

to.

10,13,33,34,35-36

structural

relations

of

31,32,33,34

thickness

of.... ._ .

4,28

Igneous

rocks,

general

features

of.

30

Kings

Gap

Spring,

analysis

of

water

of-...

17

location

of...

19

LaGrange,

Ga.,

thermal

gradient

in

well

near.

34-35

Lamar,

W.

L.,

chemical

analyses

of

water

by.

17-18

Lifsey

Spring,

analysis

of

water

of.

17

discharge

and

temperature

of

_.

_

10

geologic

relations

of .

34

location

of....

10,18

Manchester

High

School

well,

analysis

of

water

of... . .

18

chemical

character

of

water

of

15

Manchester

reservoir,

analysis

of

water

of

18

Manchester

schist,

general

features

of..

29

relation

of

warm

springs

to...

4,34

structural

relations

of____________

33,34

Mathis

well,

analysis

of

water

of .-. -.

18

Mill

Creek,

discharge

measurements

of

_

__

24

Mill

Creek

Basin,

study

of

rainfall

in. .....

35

Mountain

streams,

analyses

of

water

of___

18

Mount

Hope

Branch,

analysis

of

water

of....

18

North

Spring,

analyses

of

gases

from..___.

21

analysis

of

water

of_______...

17

discharge

of .

12,

13,

pi.

5

general

features

of____....

11-12

leoflftionof-_

11,10

temperature

of.... .

12

Oak

Mountain,

features

of.

39

40

INDEX

page

Oak

Mountain

Spring,

analysis

of

water

of_

17

chemical

character

of

water

of.._____

15

discharge

and

temperature

of.

______

14

geologic

relations

of

____________

14

location

of , ___.

________

14,19

Parkman

Spring,

analysis

of

water

of____

17

discharge

and

temperature

of_______

8

geologic

relations

of_________.,__

34

location

of

_________________

8,19

Pine Mountain,

features

of_._______

3

streams

on,

analyses

of

water

of_____

18

temperature

in

wells

near_________

4

warm

springs

near,

geologic

problems

pre-

sented

by __.___.___

1

Pine

Mountain

area,

ground-water

level

in,

observations

of_________

22,

pi.

6

ground-water

level

in,

relation

of.

to

rain-

fall.__._____.______

23,

pi.

6

rainfall

measurements

in_________

22

stream

discharge

in___.____

23,

pis.

7,

8

Pine

Mountain

divide,

comparison

of

run-off

north

and

south

of________

24-26

Pine

Mountain

formation,

occurrence

and

character

of___.________

4

Pine

Mountain

Spring,

analysis

of

water

of

17

location

of

____

_____________

19

Public

Works

Administration,

funds

allotted

by._______.____....__

1

Rainfall,

measurements

of__________

22

relation

of,

to

discharge

of

Warm

Springs.23,

pi.

4

to

fluctuations

of

groundwater

level.23,

pi.

6

weekly,

at

Roosevelt

farm_______

22,

pi.

5

Red

Sulphur

Spring,

analysis

of

water

of

___

17

location

and

general

features

of..____

14

Roan

gneiss,

occurrence

of

__________

27

Rock

formations,

general

features

of_____

25-3]

Roosevelt

farm,

rainfall

at_____

12,22,

pis.

4,5

well

on,

fluctuations

in

water

level

in.23, pis.

4,6

Run-off,

studies

of_______________

23-25

Scope

of

investigation____.________

2

Snelson

granite,

general

features

of...____

26-27

South

Spring

No.

1,

analysis

of

water

of __

.

17

South

Springs, discharge

and

temperature

of..

13

genera]

features

of _ ...__

12-13

location

of . ..._________....

32,19

Sparks

Creek,

analysis

of

water

of______

18

Sparks

schist,

general

features

of._______

27

Streams,

discharge

of________

23-25,

pis.

7,8

Structural

features_____________

31-32,33

Surface

features... ____________

2-3

Surface

waters,

analyses

of__________

18

Talbotton,

Qa.,

average

air

temperature

at__

4

rainfall

at _

22

Taylor

Spring,

analysis

of

water

of______

17

discharge

and

temperature

of_______

11

geologic

relations

of ..

34

location

of___.

_____..

____.

_

11,18

Temperature,

in

wells. _..__

34-35

of

air_____ ____ ____....

4

of

spring

water.

See

individual

springs.

Tertiary

(?)

and

later

sedimentary

rocks,

gen-

eral

features

of . __-

30-31

Thermal

gradients

in

wells... __....

34-35

Page

Thundering

Spring,

analyses

of

gases

from__

21

analysis

of

water

of... ..___.____

17

discharge

and

temperature

of..,_____

10

geologic

relations

of __ ___

34

location

of_________________

10,1&

spring

tributary

to,

analysis

of

water

of_

17

Towah'ga

fault,

pre-Cambrian

rocks

north

of.

26-27

pre-Cambrian

rocks

south

of_______

27-30

relation

of

geologic

formations

to_____

31,34

relation

of

warm

springs

to... . ..

33,34

Trammel

farm,

rainfall

at..____ __

22

Trammel's

Spring,

analysis

of

water

of.___

17

discharge

and temperature

of

13

geologic

relations

of. _

13

location

of.____._.___ __

13,19

Triassic

igneous

rocks,

general

features

of

30

Wacoochee

belt,

relation

of

warm

springs

to.

4,34

structural

relations

of

rocks

of... ___

31

Warm

Springs,

analyses

of

gases

from

21

analyses

of

water

of

17

discharge

of..

4,6-9,

pi.

4

methods

of

measurement

of

6

relation

of,

to

rainfall

and

ground-

water

level .___ ... .

23,

pi.

4

history

of

improvements

at...

4-5

measures

recommended

for

improving.;

36-37

sources

of

supply

of

5

structure

of

rocks

in

vicinity

of. .

33

temperature

of

4,5-6

water

of,

source

of..

32-33

source

of

heat

of

34-35

Warm

Springs

area,

map

of,

showing

sources

of

warm water,

pools,

drains,

etc.

pi,

3

Warm

Springs

quadrangle,

geologic

map

of

pi.

1

location

of,

map

showing

pi.

2

Warm

springs,

analyses

of

waters

of,

17

distribution

of.

3

relation

of,

to

Hollis

quartzite

36

summary

of... ^

11

Warm

waters,

chemical

character

of

15

Wells,

analyses

of

waters

of

18

temperature

of

water

of .

'

4

thermal

gradient

in.

34-35

water

levels

in s,

23,

pi.

6

West

Point,

Ga.,

average

air

temperature

at,.

4

rainfall

at........... - .-

22

White

Sulphur

Spring,

analysis

of

water

of

17

general

features

of..

14

hydrogen

sulphide

in.

16

White

Sulphur

Springs,

chemical

character

of

water

of

springs

at i

16

general

features

of

springs

at.

t

14

geologic

relations

of

springs

at

14

location

of

springs

at .

M

Willingham

Spring

No.

1,

analysis

of

water

of.

18

location

of

20

Woodbury,

Ga.,

rainfall

at

22

Woodbury

Spring

Nos.

1

and

2,

analyses

of

water

of.._

18

.

location

of -

20

Woodland

gneiss,

general

features

of

29-30

Yant,

W.

P.,

chemical

analyses

by .

21

Youngs

Mill,

Ga.,

thermal

gradient

in

well

at.

34

o

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