Low-Flow Characteristics of 

Streams in the Mississippi 

Embayment in Southern 

Arkansas, Northern Louisiana 

and Northeastern Texas

By PAUL R. SPEER, MARION S. HINES, A. J. CALANDRO, and others

With a section on QUALITY OF THE WATER

By H. G. JEFFERY

WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

GEOLOGICAL SURVEY PROFESSIONAL PAPER 448-G

The magnitude, duration,frequency of recurrence, 

and chemical composition of low flows

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1966
UNITED STATES DEPARTMENT OF THE INTERIOR 

STEWART L. UDALL, Secretary

GEOLOGICAL SURVEY 

William T. Pecora, Director

For sale by the Superintendent of Documents, U.S. Government Printing Office 

Washington, D.C. 20402
CONTENTS

Abstract. _ ________________

Introduction. _____________

Purpose and scope..___. 

Definition of terms__.

Description of the area- ____

Climate ______________

Physiography _________

Geology._____________

Manmade changes__ -.__. 

St. Francis River basinWhite River basin.___. 

Arkansas River basin. _. 

Ouachita River basin. _. 

Red River basin ... 

Farm ponds and lakes..

Page 

Gl

1

2

2

3

4

4

4

5

6

6

7

7

8

9

Page 

Low-flow characteristics-__________________--_------_ G9

Low-flow frequency-..-..-....--.--------.-- _ 13

Flow duration. __ ____________ ______

Factors affecting low flow_______-_____-__-_--_----.

St. Francis River basin__-_________--_--_-------

White River basin.. ____________________---_.---

Arkansas River basin_______________ _______

Ouachita River basin_________ _________ _.

Red River basin_______ ___________ __-

Major floods and ground-water recharge.-.--.. _ 

Low flows and ground-water fluctuations_._________--.

Method of study_____________________ ______ 

Basic data for the analysis.-.--------------- _____-.

Draft-storage relations._____________________________

Quality of the water, by H. G. Jeffery______ _

Conclusions and recommendations.__________________

Selected references..__________ __________________

ILLUSTRATIONS

17

20

21

21

21

22

24

25

26

27

27

27

31

38

39

[Plates are in pocket]

PLATE 1. Map of the study area showing generalized geology and 7-day 2-year low flow at gaging stations.

2. Map showing patterns for chemical analyses of low-flow surface waters in the study area.

FIGTTKE 1. Map of Mississippi embayment showing areas covered by four chapters of this series on low-flow character- Page 

istics of streams..______________________________________________________________________________ G3

2. Physiographic map of the study area_______________________________________________________________ 6

3. Graphs showing magnitude and frequency of annual low flow for Saline River near Rye, Ark., 1929-57____ 13

4. Graphs showing flow-duration curves for Saline River near Rye, Ark., and Bayou Bartholomew near Beekman,

La., 1929-57_____--_-_-_____________________________.___.____________________ 20

5. Hydrographs of Arkansas River and wells near Pine Bluff, Ark., 1958-59 __________________________ 26

6. Map of Mississippi embayment showing areas covered, by numbered parts, for which streamflow records are

published in reports on surface-water supply_______________________________________________________ 28

7-8. Graphs showing areal draft-storage relations in the study area:

7. Ten-year recurrence interval___________________________________________________________ 29

8. Twenty-year recurrence interval_______________.____________-_-___--__--______-__________ 29

TABLES

Page

TABLE 1. Geologic units cropping out in study area__________________________________________________________ G5

2. Low-flow characteristics of streams in the study area..____________________________________________ 10

3. Magnitude and frequency of annual low flow at daily-record gaging stations in the study area._____________ 13

4. Duration of daily flow at daily-record gaging stations in the study area__________________________________ 18

5. Chemical analyses of low-flow surface waters in the study area___________________________-__.____-_____ 32

6. Source and significance of dissolved mineral constituents and properties of water____________________ 36

m

WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

LOW-FLOW CHARACTERISTICS OF STREAMS IN THE MISSISSIPPI EMBAYMENT IN 

SOUTHERN ARKANSAS, NORTHERN LOUISIANA, AND NORTHEASTERN TEXAS

By PAUL E. SPEER, MARION S. HJNES, A. J. CALANDRO, and others

ABSTRACT

The low-flow characteristics of a stream largely govern the 

type and economics of its utilization. The magnitude, duration, 

and frequency of low flows included in this report are used both 

to determine whether a water-utilization project can be operated 

without storage, and if not, to determine the amount of storage 

required to provide the minimum flow needed.

When direct runoff from precipitation ceases, the flow of 

streams is governed by the volume of water in ground storage 

and by the rate at which the ground water discharges into the 

stream. The character and distribution of the geologic formations within stream basins exert a major influence on the quality and quantity of the low flows of streams.

Manmade changes to the land and to the stream systems probably have altered the regimen of flow of many streams.

Limited low-flow data, in cubic feet per second per square 

mile, for 50 daily-record gaging stations and 106 partial-record 

gaging stations, are summarized for ready comparison. The 

summary gives the minimum average 7- and 30-day discharges 

that may be expected to recur at 2- and 10-year intervals and 

gives the flow at the 90- and 95-percent duration points. More 

detailed data on the magnitude and frequency of low flows 

and on flow duration, in cubic feet per second, are given for 

the 50 daily-record gaging stations.

The 7-day low flows at the 2-year recurrence interval, expressed on a per-square-mile basis, are used to demonstrate 

areal variations of low flow in the study area. These low-flow 

indices range from 0 to 0.20 cubic foot per second per square 

mile.

Drafts that may be made from specified amounts of storage 

with a chance of deficiency of once in 10 or 20 years on a longterm average are related to the 7-day 2-year low flow to permit 

preliminary estimates to 'be made of the storage required to supplement natural low flows.

Chemical analyses of the surface water, as determined from 

samples collected at 36 sites during low-flow periods, show that 

the dissolved solids range from 12 to 12,900 ppm (parts per 

million) ; hardness ranges from 6 to 1,010 ppm; and the iron 

content ranges from 0.00 to 1.2 ppm. The higher values of dissolved solids and of hardness are from streams that contain 

oil-field wastes. Exclusive of these streams, the dissolved solids 

range from 12 to 855 ppm, and the hardness ranges from 6 to 

433 ppm. The surface waters in the study area generally would 

be suitable without treatment for certain uses, such as cooling, 

but for municipal and most industrial uses, the waters would 

require some treatment.

The results of the study suggest fields for further investigation to define additional phases of the hydrologic systems and 

to determine the effect that manmade changes to the stream 

systems may have on the low flows of the streams and on the 

ground^water systems.

INTRODUCTION

In the Mississippi embayment in southern Arkansas, 

northern Louisiana, and northeastern Texas, large supplies of fresh water are available from both surface 

and underground sources. The area has a high average 

annual precipitation and in addition, several major 

streams originate outside the area. The water resources 

of the area, therefore, are more than ample to meet the 

needs for many years in the future, and the anticipated 

problems in water supply are those of distribution and 

providing storage to meet the demands.

In the past, many parts of the area have been subjected to devastating floods, and much attention has 

been centered on flood control, drainage, and improving 

the channel hydraulics of the streams. In recent years, 

however, rapid economic development within the study 

area has resulted in an increased consumptive use of 

water, to the extent that serious shortages have occurred during periods of low streamflow. Knowledge 

of the areal availability of water during critical periods of low flow is paramount to the orderly economic 

growth of the area.

The flow characteristics of a stream and the chemical, physical, and biological properties of its water are 

the basis for utilizing its flow, and these factors exert 

a major influence on the economics of its development. 

These characteristics vary with time, with location, and 

with manmade changes. Of particular significance for 

utilization of a stream are the magnitude of the low 

flow, the duration and frequency of a specified discharge, and the quality of the water during the lowflow periods. The low-flow characteristics in this report include amounts of water available for use without

Gl
G2 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

storage, and these amounts also may be used to estimate 

the storage required to provide the minimum flow 

needed; included also is an indication of the chemical 

quality of the water in the streams during low flow.

Streamflow records used in the analysis for this report were collected over a period of many years by the 

U.S. Geological Survey in cooperation with the Arkansas Geological Commission, the Louisiana Department of Public Works, the Louisiana Department of 

Highways, the Texas Water Commission, and the 

Sabine River Compact Administration. Other records 

were obtained through cooperation with Federal agencies the Army Corps of Engineers, the Mississippi 

River Commission, and the Public Health Service. 

The records were processed by electronic computer in 

the Washington office of the U.S. Geological Survey 

under the direction of W. L. Isherwood, hydraulic 

engineer.

The records were analyzed and the part of this report 

that concerns streams in the three States was prepared 

by the following: For southern Arkansas and northeastern Texas, Marion S. Hines, assisted by L. D. Hauth 

and John Sullavan, under the general direction of John 

L. Saunders, succeeded by I. D. Yost, district engineer; 

and for northern Louisiana, A. J. Calandro, under the 

technical supervision of Leland V. Page, and under the 

general direction of F. N. Hansen, district engineer. 

Technical supervision of quality-of-water analyses and 

preparation of the section of the report on "Quality of 

the water" were under the direction of J. H. Hubble, 

district chemist. Other parts of the report were prepared, the results coordinated and reviewed, and the report assembled by Paul R. Speer, staff engineer. Technical guidance on analytical procedure and format was 

provided by C. H. Hardison, staff engineer. The report 

was prepared under the direction of E. M. Gushing.

The principal authors gratefully acknowledge the 

assistance of E. M. Gushing, R. L. Hosman, and A. T. 

Long, who prepared the subsection on "Geology," participated in the determination of the geologic units contributing to the low flows of the streams, reviewed the 

section on "Factors affecting low flow," and offered 

many helpful suggestions which have been incorporated 

into the report.

PURPOSE AND SCOPE

The purpose of the current phase of the investigations in the Mississippi embayment is to define the 

hydrologic systems. Because most of the area is underlain by aquifers which yield large quantities of water to 

wells, ground water is the most readily available source 

of fresh-water supply in the embayment. Surface 

waters are available to those users who have access to

the streams. In defining the hydrologic systems of the 

area, ground water and the low flows of the surface 

water are virtually one water and cannot be separated. 

The results of the studies on surface water and the results of the studies on ground water, published as 

separate chapters of this professional-paper series, 

complement each other in the definition of the hydrologic systems.

The purpose of this chapter is to present data that 

will facilitate evaluation of the characteristics of the 

low flow of the streams within the embayment in southern Arkansas, northern Louisiana, and northeastern 

Texas. It deals with surface water and with the relation 

of the underlying aquifers to low streamflow. The lowflow characteristics of streams at 156 sites in the study 

area are given in this chapter. Other chapters of this 

series contain similar data for other parts of the embayment (fig. 1).

Data essential to the planned development of water 

resources include: the magnitude of the low flow, the 

length of the period that a specific discharge continues 

or is not exceeded, the frequency at which this discharge 

recurs, and the quality of the water during the low-flow 

periods. These data also are useful in the determination 

of the recurrence of flows that are qualitatively unsuitable for specific uses and in the determination of the 

economic feasibility of designing storage capacity 

needed to produce certain minimum flows of acceptable 

minimum quality. The data included herein will enable designers to determine the magnitude and 

frequency of low flows at specific sites at the same time 

that they study the economics of development.

The data presented for specific sites consist of 

(1) frequency data showing the average intervals, in 

years, between low-flow discharges for periods of 

selected length, (2) flow-duration data showing the percentage of the reference period during which the flow 

equaled or exceeded given rates of flow, and (3) 

chemical quality of the stream water at various sites 

during low flow.

DEFINITION OF TERMS

Most of the hydrologic terms used in this report are 

defined by Langbein and Iseri (1960). Other selected 

terms, as used in this report, are defined as follows:

Aquifer. A formation, group of formations, or part 

of a formation that is water bearing.

Climatic year. The year beginning April 1 and ending March 31 of the following calendar year.

Low-flow frequency curve. A graph showing as 

abscissa the recurrence interval (average return 

period), in years, at which the lowest mean flow for a 

selected number of days during a climatic year may be
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G3

expected to be no greater than a specified discharge, 

plotted as ordinate.

Low-flow index. The median annual 7-day low flow, 

in cubic feet per second per square mile.

Median annual 7-day low flow. The annual 7-day 

low flow having a recurrence interval of 2 years (7-day 

2-year low flow); that is, the mean flow for 7 consecutive days to be expected as an annual minimum 1 year 

out of 2, on the average.

Partial-record station. A particular site on a stream 

at which limited streamflow data, usually consisting of 

sufficient streamflow measurements to establish a lowflow relation with the daily record at a nearby station, 

are collected over a period of years for use in hydrologic 

analyses.

DESCRIPTION OF THE AREA

The area of the embayment covered by this chapter 

(fig. 1) includes 21,000 square miles in southern Arkansas, 11,100 square miles in northern Louisiana, and 4,000 

square miles in northeastern Texas.

Drainage from the area is to the Mississippi Eiver 

and its tributary basins. The principal tributary 

basins are Bayou Bartholomew and the lower ends of 

the St. Francis, White, Arkansas, Ouachita, and Red 

Rivers. The natural stream patterns are extremely irregular and meandering. The channels have fairly 

flat slopes and are interspersed with abandoned channels and water courses. The streams are sluggish. 

Many of the channels have been altered by man to 

facilitate drainage of the land and to improve the 

hydraulics of the channels.

33° 

32

FIGURE 1. Map of Mississippi embayment showing areas covered by four chapters of this series on low-flow characteristics of streams.

covered by this chapter is shaded.

Area
G4 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

The Bed River is distinctive in the area in that it occupies a structural depression analogous to that of the 

Mississippi Eiver (Fenneman, 1938, p. 115). The sediment load of the Red River and the extensive forested 

areas in the basin have made the river subject to clogging by driftwood which, in the past, has formed 

"rafts" in the channel. The last of these, the Great 

Raft, probably began in the 15th century and before its 

removal in 1873 had created a lake 160 miles long extending upstream almost to the Arkansas line. The effects of these obstructions were: to build a broad 

alluvial flood plain; to create lakes 5 to 25 miles long, 

such as Lake Bistineau, in the tributary valleys; and to 

force the Red River to adopt new courses at various 

places.

CLIMATE

The climate of the area is warm and humid. The 

average annual precipitation ranges from about 48 to 

52 inches. Nearly all of the precipitation is in the form 

of rain, but measurable snowfall does occur. The area 

lies in the paths of the rain-producing storm centers 

that move northeastward off the Gulf of Mexico and the 

dry continental airmasses that move west to east across 

the continent. Occasionally a cold airmass invades as 

far south as northern Louisiana, becomes stationary, 

and produces prolonged rains. The temperatures 

range from an average low of about 32°F during 

January in central Arkansas to an average high of 

about 96°F during July in northeastern Texas.

PHYSIOGRAPHY

The Mississippi embayment, a part of the Coastal 

Plain province, is an extensive lowland in a great 

structural trough between the Appalachian and Interior Highlands (Fenneman, 1938, p. 96). It has been 

formed by subsidence of the trough, aggradation, differential weathering, erosion, and crustal movement. 

During much of its existence, the embayment has been 

submerged by the sea, and since the embayment last 

emerged, the Mississippi River has followed close to the 

axis of the trough. Figure 2 shows the large physiographic districts in the area covered by this report.

The St. Francis Basin, north of the Arkansas River, 

and the Tensas Basin, south of the Arkansas River, occupy a belt ranging from about 30 to 100 miles wide 

that lies west of the Mississippi River. The basins are 

fairly flat flood plains of Quaternary age, interspersed 

with sluggish, meandering streams. Crowleys Ridge, 

in the St. Francis Basin near the northeast corner of the 

area, is composed of Tertiary deposits capped by Quaternary sediments and rises 100 to 150 feet above the 

alluvial plain of the St. Francis Basin. In the geologic 

past, Crowleys Ridge was a major divide between two 

great rivers that contributed to the aggradation of the 

alluvial plain of the embayment. The Grand Prairie 

region is the local name for that part of the St. Francis 

Basin in Arkansas that lies between Bayou Meto and 

the White River and extends from about Wattensaw 

Bayou on the north to the Arkansas River on the south.

The East Texas Timber Belt lies primarily on the Tertiary and occupies most of the study area west of the St. 

Francis and Tensas Basins. The topography is fairly 

flat, but is slightly more expressive than that in the 

St. Francis and Tensas Basins.

The Black Prairie in northeastern Texas covers the 

Upper Cretaceous except for the basal (Woodbine) 

sands (Fenneman, 1938, p. 103).

The area of the Mississippi embayment in southwestern Arkansas is marked by three cuestas. The northernmost of these, the Lockesburg Wold, is the bordering 

belt of low sand-and-gravel hills and uplands (Fenneman, 1938, p. 107) of the lower part of the Upper 

Cretaceous. South of the Lockesburg Wold, the Saratoga Wold is underlain by the Nacatoch Sand of late 

Cretaceous age; farther south, the Sulphur Wold is on 

the zone of the sandy Wilcox beds of Eocene age.

GEOLOGY

The area covered by this report was periodically 

occupied by the sea in the geologic past and has been 

filled by sediments ranging in age from Jurassic to Quaternary. These deposits are several thousand feet thick 

near the axis of the embayment in the southeastern part 

of the area, and they gradually thin updip to the north 

and northwest toward the margin of the embayment. 

Units ranging in age from Cretaceous to Quaternary 

crop out within the area (pi. 1), and Paleozoic rocks 

ranging from Ordovician to Pennsylvanian crop out 

along the periphery of the embayment. Cushing, Boswell, and Hosman (1964) give a general description of 

the units of Cretaceous age and younger.

The major geologic units that crop out in the area of 

study are given in table 1. The sand units, which contribute most of the water to the base flow of streams, 

include the Trinity Group, the Woodbine and Tokio 

Formations, the Wilcox Formation or Group, the Carrizo Sand, the Mount Selman Formation, the Sparta 

Sand, the Cockfield Formation, and the alluvium and 

terrace deposits.
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G5

TABLE 1. Geologic units cropping out in study area

Northeastern Texas

(Bowie, Cass, Marion, and Harrison Counties) 

Quaternary System

Alluvium and terrace deposits 

Tertiary System 

Eocene Series

Claiborne Group 

Sparta Sand 

Mount Selman Formation

Weches Greensand Member 

Queen City Sand Member 

Reklaw Member 

Carrizo Sand 

Wilcox Formation 

Paleocene Series 

Midway Group

Wills Point Formation 

Kincaid Formation 

Creaceous System

Upper Cretaceous Series

Navarro Group undifferentiated 

Taylor Marl 

Annona Chalk

Northern Louisiana

(North of 32d parallel) 

Quaternary System

Alluvium and terrace deposits 

Tertiary System 

Eocene Series

Claiborne Group

Cockfield Formation 

Cook Mountain Formation 

Sparta Sand 

Cane River Formation 

Carrizo Sand

Eocene and Paleocene Series 

Wilcox Group l

Dolet Hills Formation 

Naborton Formation

Northern Louisiana Continued 

(North of 32d parallel)

Paleocene Series 

Midway Group

Porters Creek Clay 

Clayton Formation

Arkansas

Quaternary System

Alluvium and terrace deposits 

Loess 

Tertiary System

Pliocene (?) deposits 

Eocene Series

Jackson Group undifferentiated 

Claiborne Group

Cockfield Formation 

Cook Mountain Formation 

Sparta Sand 

Cane River Formation 

Carrizo Sand

Wilcox Group undifferentiated 2 

Paleocene Series

Midway Group 3

Porters Creek Clay 

Clayton Formation 

Cretaceous System

Upper Cretaceous Series 

Arkadelphia Marl 

Nacatoch Sand 

Saratoga Chalk 

Marlbrook Marl 

Annona Chalk 

Ozan Formation 

Brownstown Marl 

Tokio Formation 

Woodbine Formation 

Lower Cretaceous Series

Trinity Group undifferentiated 

Paleozoic rocks undifferentiated

i Wilcox Group (Eocene Series) undifferentiated. Wilcox Group (Paleocene Series), upper part undifferentiated; Dolet Hills and 

Naborton Formations are lower two units.

' In ascending order, Wilcox Group in Arkansas bauxite area is composed of Berger Formation, Saline Formation, and Detontl 

Sand.

' In ascending order, Midway Group in Arkansas bauxite area is composed of Kincaid Formation and Wills Point Formation.

MANMADE CHANGES

Settlers brought about changes in the area that probably have affected the low flows of the streams. These 

changes may be divided into two groups: (1) changes 

applied to the land in converting it to man's beneficial 

use, such as irrigation, drainage, land utilization, urban 

development, changes in agricultural crops, and intensity of cultivation, and (2) changes in the stream systems, such as diversions, development of levees, 

construction of dams for impounding water, and 

changes in stream channels. Some changes were begun 

before records of streamflow were obtained in the area, 

and others have been made so gradually that, even if

7&3-I634 66 2

the effects could be isolated, it would require many subsequent years of record to define them.

Many streams in the embayment in southern Arkansas, northern Louisiana, and northeastern Texas are 

affected by manmade changes. Water is diverted to 

and from the streams, channels have been dredged, 

levees have been constructed, large areas have been 

drained, and dams have been built for flood protection, 

for recreational facilities, and to make water available 

for agricultural, municipal, or industrial uses.

The effects of many manmade changes are not permanent. Dredged channels may become partially filled 

with sediment, or they may erode deeper due to increased
G6 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

FIGURE 2. Physiography of the study area. After Fenneman (1938) and others.

velocity of flow. Channel clearing and snagging are 

temporary improvements because of the regrowth of 

vegetation and reaccumulation of debris. On the other 

hand, major reservoirs that have been created on many 

of the streams have material effects of a permanent 

nature on downstream flows. Attempting to describe 

all the manmade changes or to evaluate quantitatively 

the effects that they may have produced on the streamflow is beyond the scope of this report, but some of the 

major changes that may aid interpretation of the lowflow characteristics are described briefly in the following paragraphs. The major part of the information 

was obtained from publications of the Corps of 

Engineers.

ST. FRANCIS RIVER BASIN

Low flows of the St. Francis River have been affected 

by regulation at Wappapello Reservoir in Missouri 

since 1941, by operation of the locks and siphons at

Marked Tree, Ark., since 1925, and by numerous drainage projects in the basin. Channel cutoffs have been 

dredged and other channel improvements completed 

along the lower St. Francis River. The L'Anguille 

River channel has been cleared for about 5 miles upstream from the mouth as part of the St. Francis River 

basin project. Additional channel and drainage improvements are proposed (1964) for both the St. 

Francis and L'Anguille Rivers.

WHITE RIVER BASIN

The low flows in the lower end of the White River 

are regulated by six reservoirs, the first in operation 

being the Norfork Reservoir in 1943. Construction of 

the dam for a seventh reservoir was started in 1961. 

Rarely, the daily discharge of the lower White River 

may be affected also by leakage and unusual operations 

at locks and smaller dams upstream.
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G7

Some levee and channel-improvement work has been 

done along the lower White Eiver and its tributaries. 

Extensive channel improvements have been proposed 

for approximately 195 miles of Cache River and approximately 90 miles of Bayou De View.

ARKANSAS RIVER BASIN

Efforts to improve the Arkansas River began as early 

as 1832. Early projects by the Corps of Engineers and 

municipal agencies were primarily to protect towns and 

cities from floods, to prevent erosion of the riverbanks, 

and to improve navigation. Dikes were constructed to 

direct the flow, and revetments were installed to prevent scour and to stabilize the banks. The Arkansas 

River enters the Mississippi embayment at Little Rock, 

Ark. From this point to the mouth, levees have been 

built at several points along the river, and cutoff channels have been dredged to bypass some of the more 

tortuous bends. At least seven such cutoffs, some of 

which shortened the channel as much as 6 miles, were 

constructed during the period 1952-56. Some levee 

work has been done on tributaries upstream from Little 

Rock, such as in the Spadra Creek project, which may 

affect the low flow of the Arkansas River within the 

embayment by limiting the area and frequency of flooding of the alluvial valley.

Numerous diversions for irrigation and the operation 

of many reserviors throughout the Arkansas River basin 

have greatly altered the low flows of the Arkansas River. 

The Corps of Engineers is presently engaged (1964) in 

a multiple-purpose project which combines the development of flood control, navigation, hydroelectric power, 

and related facilities on the Arkansas River and tributaries. Under this plan, navigation will be provided 

from the Mississippi River upstream into Oklahoma. 

The project includes the creation of seven reservoirs in 

eastern Oklahoma and two in western Arkansas.

In the Grand Prairie region (fig. 2), irrigation is 

probably the major operation affecting the low flow of 

the streams. Ricefields are alternately flooded and 

drained during the growing season, and most of the 

irrigation water that is derived from ground water is 

not returned to the ground, but is either lost by evapotranspiration or is diverted to the streams. As a result 

of heavy pumping of water from the Quaternary aquifer, the ground-water table along the Arkansas River 

in parts of Lincoln, Jefferson, and Arkansas Counties slopes away from the river, and this condition 

probably causes some of the flow in the Arkansas to 

be diverted into the ground water in this reach of the 

channel. Overdevelopment of ground-water supplies 

in the Grand Prairie region is shifting the emphasis on 

water supply to surface-water sources.

In the Grand Prairie region and in the Bayou Meto 

basin, a project is authorized for the Corps of Engineers 

to do channel-improvement work on Bayou Meto, Little Bayou Meto, Salt Bayou, Wabbaseka Bayou, and 

Bradley Slough to provide for flood control and drainage and to supply supplemental water for agricultural 

purposes in the Grand Prairie region. Only the preliminary planning has been done on this project to date 

(1963).

OUACHITA RIVER BASIN

Low flows of the Ouachita River have been affected 

by storage in Lake Ouachita since 1952, Lake Hamilton 

since 1932, and Lake Catherine since 1925, all in the 

vicinity of Hot Springs, Ark., and by storage in Lake 

Greeson on the Little Missouri River since 1949. Upstream from Lake Ouachita, there is no known regulation affecting low flows.

A 6.5-foot channel is maintained on the Ouachita 

River from Camden, Ark., to the mouth. Six locks and 

dams below Arkadelphia, two of which are in Arkansas, 

may cause some regulation, but the effect on daily flow 

is considered to be of no consequence. The Corps of 

Engineers has under construction a project which provides for a 9-foot channel and new locks and dams to 

replace locks and dams 2 to 8. Work on the 9-foot 

channel from Camden to Arkadelphia, Ark., is now 

inactive (1965).

Some channel-improvement work has been completed 

on Little Missouri River below Murfreesboro, Ark., on 

Ozan Creek from the mouth to 15 miles upstream, and 

on Terre Noire Creek from the mouth to 24.4 miles upstream. Most of this work is being done under current 

projects. Similar work has been done on other tributary streams under previous projects, but information on this work is not readily available.

There have been no channel improvements or enlargements in the Bayou Bartholomew basin during the period of record on this stream. Water is diverted each 

year during the growing season above the gaging station near Beekman, La. (7-3645), for irrigation of approximately 1,000 acres of rice. Chemin-a-Haut Lake 

(capacity, 150 acre-ft) on Chemin-a-Haut Bayou, tributary to Bayou Bartholomew upstream from Beekman, was created in 1949.

Considerable channel-improvement work was done in 

the Boeuf River, the Tensas River, and the Bayou 

Macon basins during 1942-56 by the Corps of Engineers 

and by the Louisiana Department of Public Works. 

This work mostly resulted in the deepening and 

straightening of the channels. The Boeuf River channel is to be shortened 3.6 miles when the remainder of the 

cutoff and realinement work in Chicot County, Ark., is
G8 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

finished. Canals 18, 19, 43, and 81 in the Boeuf River 

basin are undergoing improvements (1963). A small 

amount of channel-improvement work is being done on 

Bayou Macon in Chicot County, Ark.

The Louisiana portion of work in the Boeuf River, 

Tensas River, and Bayou Macon basins by the Corps of 

Engineers consists of the clearing, snagging, straightening, and enlarging of approximately 530 miles of channel on the Boeuf River, the Tensas River, Bayou La 

Fourche, Bayou Macon, Big Creek, and Big Colewa 

Bayou. Improvements on about 288 miles were completed as of June 1956. The Louisiana Department of 

Public Works cleared, enlarged, and realined channels 

in 13 bayous during the period 1949-57. The Bayou La 

Fourche cutoff loop was completed in 1956 to provide a 

larger outlet into the Boeuf River.

There have been no channel improvements in Bayou 

D'Arbonne basin during the period of records. Corney 

Lake (capacity, 28,000 acre-ft) on Corney Bayou above 

the gaging station near Lillie, La. (7-3660), was created 

in 1940.

Cheniere Brake Lake (capacity 15,000 acre-ft) on 

Cheniere Creek, which is a tributary of the Ouachita 

River 13 miles downstream from Monroe, La., was 

created in 1944.

Information from the Louisiana Department of Public Works indicates that very few, if any, channel improvements have been made in Dugdemona River basin. 

Water for industrial use is pumped from wells at 

Hodge, La., and part of the effluent is discharged continuously into the Dugdemona River about 7 miles above 

the gaging station near Jonesboro, La. (7-3715). The 

effluent, which contains waste material, is stored in a 

reservoir and released when the riverflow is sufficient 

to materially dilute the effluent.

The Soil Conservation Service projects in the 

Ouachita River basin included the Randolph-Walnut 

Lake project in Desha County, Ark., completed in 1961, 

which provided for the improvement of 24 miles of 

drainage channel which is tributary to canal 19 near 

Dumas; the Arkansas City project in Desha County, 

completed in 1963, which provided for the improvement 

of 23 miles of channel on a tributary to canal 81; and 

the improvement of 28 miles of channel on Camp Bayou 

and on laterals near Wilmot, Ashley County, Ark., 

completed in 1959.

RED RIVER BASIN

Channel improvements and levee projects have been 

completed at many places along the Red River and on 

several tributaries. The banks and channel of Walnut 

Bayou have been improved from the Oklahoma line to 

the mouth. The flow of McKinney Bayou and its tributary, Barkman Creek, is diverted into the Red River 

3 miles west of Ogden, Ark. Levee construction and 

channel improvement have been completed on McKinney Bayou from near Texarkana to the mouth. Downstream from Ogden, on the Red River, 159 miles of levees 

on the left bank, 235 miles of levees on the right bank, 

and 14.2 miles of revetment or bank protection have 

been built.

Several small lakes and reservoirs have been created 

on the Red River and tributaries west of the embayment. 

Lake Texoma created by Denison Dam on the Red 

River near Denison, Tex., impounds runoff from 39,719 

square miles. Six major reservoirs on tributaries of the 

Red River below Denison Dam have been or are being 

created (1963).

Work on the Sulphur River and tributaries in Texas, 

consisting of the construction of levees, the improvement and straightening of the channel, and the removal 

of accumulated snags and other debris, has been completed on the main stem above Lake Texarkana, on the 

North, Middle, and South Sulphur Rivers, and on 

Journigan, Cane, Mustang, and Cuthand Creeks. Lake 

Texarkana (capacity, 119,700 acre-ft) was created in 

1957 for flood control and water conservation.

Lake O' the Pines (capacity, 842,100 acre-ft), on 

Cypress Creek about 8 miles west of Jefferson, Tex., was 

created in 1958. Between Jefferson, Tex., and Shreveport, La., dredging and straightening the channel, removing obstructions, and clearing banks have been 

completed on 66 miles of Cypress Creek.

Downstream from the Arkansas line, there are a number of depressions near the mouth of the tributaries 

of the Red River which were occupied by lakes created 

by the Great Raft before its removal (p. G4). Some 

of these depressions have been utilized for the creation 

of lakes for flood-control, water-supply, and recreational purposes.

Black Lake (capacity not known), on Black Bayou 

upstream from the gaging station near Gilliam, La. 

(7-3475), was created in 1945 for recreational purposes. 

In 1955, the crest of the dam was raised to enlarge the 

lake to a capacity of 17,750 acre-ft. Water is pumped 

from Red River into Black Bayou basin downstream 

from Gilliam for the supplemental irrigation of approximately 600 acres.

The channels of Kelly Bayou and many of its tributaries were cleared, enlarged, and realined in 1943 by 

the Louisiana Department of Public Works. During 

dry periods each year, approximately 600 acres of croplands is irrigated, using water diverted from Kelly 

Bayou downstream from the gaging station near 

Hosston, La. (7-3470).
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G9

Caddo Lake (capacity, 170,000 acre-ft), 5.5 miles 

above the gaging station on Twelvemile Bayou near 

Dixie, La. (7-3480), was created in December 1914 for 

navigation and irrigation purposes. It provides a 4- 

foot navigable depth upstream to Jefferson, Tex. Each 

year water is pumped from Twelvemile Bayou upstream from Dixie for irrigation of approximately 200 

acres of land. Cross Lake (capacity, 9,920 acre-ft) on 

Cross Bayou, a tributary to Twelvemile Bayou 16 miles 

downstream from Dixie, was created in 1925 for municipal water-supply, flood-control, and recreational 

purposes.

Wallace Lake (capacity, 96,100 acre-ft), a flood-control reservoir on Wallace Bayou, was created in 1946.

The enlarging, snagging, and clearing of 21 miles 

of the channel of Bayou Pierre from near Shreveport, 

La., downstream to the mouth of its right-bank tributary, Wallace (Cypress) Bayou, were completed in 

1950. The improvement of the lower 30 miles of Bayou 

Pierre channel was completed in 1939.

Lake Bistineau (capacity, more than 120,400 acre-ft) 

on Bayou Dorcheat downstream from the gaging station near Minden, La. (7-3490), was created in 1943 

for recreation.

Channel improvements, which consisted of 2.4 miles 

of channel snagging and clearing and 5.4 miles of 

channel enlargement on Bodcau Bayou downstream 

from the gaging station near Sarepta, La. (7-3495), 

and on Red Chute and Loggy Bayous, were completed 

in 1948. Bodcau Lake (capacity, 357,300 acre-ft), a 

flood-control reservior downstream from Sarepta, was 

created in 1948. Ivan Lake (capacity, approx. 5,000 

acre-ft) on Caney Creek, which is a tributary to Bodcau 

Bayou about 7 miles downstream from Sarepta, was 

created in 1957 for recreation. Water used by a papermill upstream from Sarepta is pumped from wells and 

later discharged into Bodcau Bayou. The effluent is 

stored in a reservoir and released when the flow of the 

bayou is sufficient to dilute the waste.

Channel improvements, which included the clearing, 

enlarging, and realining of the channels of Black Lake 

Bayou and some of its tributaries, were completed in 

1949 by the Louisiana Department of Public Works. 

Kepler Creek Lake (capacity, 14,500 acre-ft), on a 

tributary to Black Lake Bayou upstream from Castor, 

La. (7-3525), was created for recreation in 1958.

FARM PONDS AND LAKES

The U.S. Department of Agriculture has assisted in 

the creation and improvement of many small ponds in 

the study area. Many other water impoundments have 

been created by other agencies, individuals, and private 

organizations. The Arkansas Conservation Needs

Committee estimates that there are presently 26,200 

farm ponds and lakes, 40 acres or less in size, in the 

Mississippi embayment in Arkansas. It is estimated 

that more than 5,600 small impoundments having a total 

capacity of about 60,000 acre-ft were created in northern 

Louisiana during the period 1938-55.

Listed below are those lakes covering 1,000 acres or 

more, excluding those mentioned elsewhere in this section, that are in the Mississippi embayment in Arkansas 

and Texas:

Area 

Lake Stream County (acres)

Arkansas:

Chicot_________ Connerly and Ferry Bayou.. Chicot__- .. 4,124 

Grassy..__._.._ Yellow Creek,..._....__ Hempstead.. 3,600

Horseshoe-._____ Fish Bayou and Boggy Bayou Crittenden 1,904 

Melwood Old River_ Mississippi River..__...... Phillips.. . 1,240

Old River 66.__.__ _.do....___________ .... do........ 3,030

Old Town_._____ McGhee Bayou. __._ ..-.dp. 4,000 

Peckerwood..____ Lagrue Bayou____ _ Prairie. 3,166 

Earling_.______ Bodeau Creek________ Lafayette.... 7,000

Seven Devils.____ Cutoff Creek.__ ... ... Drew.. 2,500 White Oak.._.___ Whiteoak Creek...___._ Ouachita..... 2,600

Texas:

Lake Cherokee. ___ Cherokee Bayou_-__ _ Rusk.... 3,479

The effect of most of these impoundments on streamflow is extremely local, but the very large number of 

small ponds in certain areas may influence the low-flow 

characteristics of some streams, and the effect of the 

ponds should be considered in the low-flow appraisal of 

streams within a basin.

LOW-FLOW CHARACTERISTICS

Streamflow data used in this report are (1) continuous records of flow obtained at 50 daily-record gaging 

stations, and (2) limited data collected systematically 

over a period of years at 106 low-flow partial-record 

stations.

So that the low-flow characteristics of one stream 

could be compared with those of another, all data were 

adjusted to the common reference period, 1929-57. 

(See section on "Method of study" for further discussion on the reference period.) In the area, 5 dailyrecord gaging stations have complete records for the 

selected period, and 39 other daily-record stations have 

15 years or more of record during the reference period. 

Daily-record stations having less than 5 years of record 

during this period are designated as partial-record stations. Data recorded through 1963 were used to define 

the low-flow characteristics at partial-record stations.

Average annual precipitation in Arkansas and northern Louisiana from 1891 to 1957 was about 49 inches, 

and that from 1929 to 1957 was 48.6 inches. Thus, the 

average during the reference period was approximately 

equivalent to that since 1891. The spatial and withinthe-year distribution of precipitation and many other 

factors, however, influence the quantity and rate of runoff, so that firm conclusions on the representativeness of 

Streamflow patterns during the reference period cannot 

be drawn from the average precipitation alone.
G10 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

The low-flow characteristics for all streams analyzed 

in the study are summarized in table 2. The stations 

are all in Part 7 except Sabine River at Logansport, 

La., which is in Part 8, and are listed in the downstream order corresponding to that currently used by 

the U.S. Geological Survey in surface-water reports. 

The station number is the permanent nationwide number assigned to the station and is used throughout the 

report. In assigning the numbers, no distinction is 

made between daily-record stations and partial-record

stations. For some of the stations for which three or" 

more of the selected items are zero flow, additional flow1 

data are given in parenthesis with appropriate reference notes.. The last column of the table enables the 

user of the data to construct the relation curve between 

the partial-record station and the daily-record station 

and to interpolate additional data if desired. Some of 

the partial-record stations were related with other 

partial-record stations; for each such station the number of the other station is shown in parenthesis.

TABLE 2. Low-flow characteristics of streams in the study area

[Data are adjusted to period 1929^57 on basis of relation to data at other gaging stations. Class of station: D, daily-record gaging station; P, partial-record or short-term 

daily-record station. Figures given for the 7-day 2-year annual low flow are the indices of low flow used in this report]

Station Station name

Class of station

Drainage 

area 

(sqmi)

Annual low flow, in cubic feet per second per 

square mile, for indicated period of consecutive days and for indicated recurrence interval, 

in years

7-day

2-yr 10-yr

30-day

2-yr 10-yr

Flow, in cubic feet 

per second per square 

mile, which was 

equaled or exceeded 

for indicated percent 

of time

90 95

Daily-record 

station with 

whichjpartialrecord station 

is correlated »

Part 7. Lower Mississippi River basin

7-0479.2___.._. 

0479.4.......

0479.5.. 

0768-..-...

0768.5.......

0769.5.. 

0779.5... 

0779.7 

0780.-.. .

2636........

2640. .

2642........

2645........

2652..... 

3369.. ......

3369.5 

3395........

3400 _ . __

3405........

3410........

3421.5 

3423.5 __ 

3425.., ..

3430.. .

3432........

3435 

3440... .

3441

3443... ..

3445 _ 

3450. 

3460- 

3460. 2_ 

3460.4. ..

3460. 6. 

3460.8 

3461. .

3461.2. 

3461. 4_ 

3463.2. ..

3464. 

3465. 

3470 

3476 __ 

St. Francis River basin

Fifteen Mile Bayou near West Memphis, 

Ark.

White River basin 

Bayou des Arc near Garner, Ark ..........

Arkansas River basin

Bayou Meto near Lonoke, Ark. _____

Red River basin 

Walnut Bayou near Foreman, Ark __ _

Manice Bayou near Canfleld, Ark ____

Kelly Creek near Marietta, Tex ...........

Hughes Creek near Avinger, Tex .........

Moccasin Creek near Harleton, Tex .......

Black Bayou near Atlanta, Tex .... .

Black Bayou near Gilliam. La ._. 

P 

P

D

P

P

P

P

P

D

P

P

P

D

P

P

P

D

D

D

D

P

P

D

D

P

D

D

P

P

D

D

D

P

P

P

P

P

P

P

P

P

P

D

D

51.0 

503

807

97.1

163

195

389

125

175

162

203

14Q

560

450

83.6

31.5

181

2,674

361

124

109

169

527

276

1,365

404.

2,774

18

12.2

366

72

850

50.5

48.6

30.5

29.5

27

83

47.9

52.1

113

231 lie

364

0 0. 012) 

(>. 032)

0-029)

0.017)

0

.001

0.021)

.001

.001

.001

.010

.001

0

0

0.001)

0.009)

.002

.007

.019

.001

.002

0

0

0

0

.001

.001

0.023)

0.020)

.002

0. 001)

.005

0. 001)

0.008)

0.004)

.003

0

0

.001

.002

.003

.002

.02

.02

0 

0

0

0

0

0

0

0

0

0

.001

0

0

0

0

0

0.001)

.001

.005

0

O.ooi)

0

0

0

0

0

0

0

0

0

0

(*. 001)

0

0

0

.001

0

0

0

0

.001

0

.02

.009

0.005 

0. 015)

.012

.004

(2.002)

.002

.008

.005

.007

.004

.019

.003

.001

0

0.003)

.007

.007

.015

.030

.002

.003

0

0.001)

(1 004)

0

.001

.002

.016

.013

.006

0.008)

.008

0.029)

.001

.001

.005

0

0

.001

.003

.004

.004

.03

.02

0 

0

0

0

0

0

0

0

.001

0.001)

.004

0

0

0

0

0

.001

.002

.008

0

.001

0

0

0

0

0

0

0

0

0

0

0. 002)

0

0

0

.001

0

0

0

0

.002

.001

.02

.01

0.008 

.022

.019

.003

P. 007)

.002

.014

.008

.009

.005

.018

.002

0

0

0.009)

.016

.036

.003

.005

.001

0.001)

0.001)

O.ooi)

.001

.002

0-023)

0.020)

.004

0.001)

.008

0. 002)

0.010)

0.004)

.008

0.002)

0.027

.003

.007

.003

.002

.03

.02

0 

.001

.001

0

0

.001

0

.001

.001

.001

.009

.001

0

0

0

0

.002

.006

.022

.002

.002

0

0

0

0

.001

0

0

0

0

0

.003

0

0

0

.003

0

0

.001

.002

.002

.001

.02

.01

7-0479.5 

7-0479.5

7-0760

7-0760

7-0775

7-0479.5

7-3630

7-3630

7-0775

7-0775

7-3635

7-3460

7-3450

7-3658

7-3658

7-3386

7-3460

7-3450

7-3445

7-3445

7-3460

7-3658

7-3658

7-3490

7-3668

7-3658

7-3475

7-3475

See footnotes at end of table.
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS 

TABLE 2. Low-flow characteristics of streams in the study area Continued

Gil

Station Station name

Class of stationDrainage 

area 

(sqmi)

Annual low flow, in cubic feet per second per 

square mile, for indicated period of consecutive days and for indicated recurrence interval, 

in years

7-day

2-yr 10-yr

30-day

2-yr 10-yr

Flow, in cubic feet 

per second per square 

mile, which was 

equaled or exceeded 

for indicated percent 

of tune

90 95

Daily-record 

station with 

whicht>artialrecordstation 

is correlated >

Part 7. Lower Mississippi River basin Continued

7-3480- 

3482.. _ ...

3486 _ -

3487.. ...

3487.6. 

3488 _ .....

3489 _ .....

3490. -.

3491- 

3492... 

3494.3. 

3495. .

3496. _ ....

3496.5. 

3498. 

3498.4......

3500 

3510 __ 

3515- 

3515.5 

3516.7. 

3517 

3517.2 __ ...

3517.6... .

3520.. ......

3521 ___ ..

3522.. ......

3522.5... _ .

3523 _ .....

3523.5.......

3524 

3525..- 

3526....- 

3527 __ 

3527.5... 

3528.. 

3530.... 

oeari

3587-. 

3596........

3598 

3601 

3602.... 

ocfwj

3610 __ ....

3612..... _

3615 

3616.5 

3617 _ .....

3618.. __ ..

3618.5 - ...

3619... 

3621 

3625 

3625.5. 

3626 _ .....

3627........

3628-... 

3629 

3630 _ .....

3631..... 

3633... 

3635 

3637 ___ -

3640.2 __ ...

3640.6 .......

3641.5 

Red River basin Continued

Bayou Dorcheat near Buckner, Ark .......

Black Bayou at Leton, La. _ __ _. _.

Flat Lick Bayou near Leton, La. . ..

Brushy Creek near Sibley, La. . __ ..

Bodcau Creek at Stamps, Ark. ___ ..

Cypress Bayou near Benton, La. __ . ...

La. 

Rambin Bayou near Frierson, La _ ....

Buffalo Bayou near Naborton, La .........

Bayou Terre Blanc near Alien, La ........

Saline Bayou near Lucky, La ____ ....

Saline Bayou near Goldonna, La. .........

Black Lake Bayou near Minden, La. ......

Bear Creek near Ada, La ___ .. .......

Black Lake Creek near Gibsland, La ......

Leathermans Creek near Gibsland, La __

Kepler Creek near Sparta, La _ ..._._ 

Mill Creek near Castor, La ................

Castor Creek at Castor, La ________

Brushy Creek near Liberty, La ...........

Grand Bayou near Coushatta, La. ........

Ouachita River basin

Gulpha Creek near Hot Springs, Ark _ ..

Caddo River at Caddo Gap, Ark .........

L'Eau Frais Creek at Joan, Ark ...........

Ark. 

Ozan Creek near McCaskill, Ark ..........

Terre Rouge Creek near Prescott, Ark ....

Caney Creek near Bluff City, Ark ...___..

Terre Noire Creek near Gurdon, Ark .....

Tulip Creek near Pine Grove, Ark ........

Bayou Freeo near Eagle Mills, Ark ........

Sinackover Creek near Smackover, Ark ...

Alum Fork at Crows, Ark ................

Middle Fork at Crows, Ark ________

South Fork near Hot Springs, Ark ........

Francois Creek near Poyen, Ark ..........

Hurricane Creek near Sheridan, Ark ___

Q&lirlA *Riir0l* nt *Rvp Arlr

Eagle Creek at Hermitage, Ark ...........

Bayou Bartholomew near McGehee, Ark..

D

P

P

P

P

P

P

D

P

P

P

D

P

D

P

P

D

D

D

D

P

P

P

P

D

P

P

P

P

P

P

D

P

P

P

P

D

D

P

P

D

P

P

D

D

P

D

P

P

P

P

P

P

D

P

P

P

P

P

D

P

P

D

P

P

P

P

3,137

78

101

605

49.8

66.9

16.1

1,097

43.6

35.1

234

546

63.9

683

133

17.2

2,628

79

66

266

59.6

19.5

17.7

26.6

154

293

38.6

53.1

46.1

57

21.1

423

21.5

27.9

13.3

93.9

1,386

410

50.2

115

312

79.4

66.5

380

148

231

167

250

152

94.8

377

216

374

123

109

12.9

132

569

84.1

205

2,062

90.3

167

93.3

592

0.003

0

(2.002)

0

(2. 002)

.001

0

.001

.01

(2.003)

0

.001

0

(2. 001)

0

.007

(2. 001)

(2.002)

(».001)

0

.04

0

0

.07

.09

.004

.001

(>.003)

.004

.20

.03

.08

.16

.005

(>.002)

.005

039

.028

.15

.077

.020

.19

.020

(*. 004)

001

.001

(>.004)

.001

.009

.001

.012

0

0

.010

.033

.071

.005

.021

.001

.007

.013

0

0

(«)

.022

0.002

0

0

0

0

0

0

0

005

(*.001)

0

0

0

0

0

0

.001

0

0

0

0< > («) («)

.035

.04

.001

0

0

.002

.16

.02

.05

.12

.001

0

0

.014

.009

.077

.038

.005

.11

0

.008

0

{<. 001)

0

0

0

< )

0

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0

0

.002

.009

.022

.001

.005

0

.001

.004

0

0

(«)

.008

0.005

0

(2.006)

0

(2.008)

.001

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(4.007)

(2.006)

.001

0

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(2.003)

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(».001)

.05

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.21

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(>.003)

.01

.063

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.20

.10

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.23

.001

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(».051)

.002

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.001

.014

0

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.11

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.035

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0

0

(«)

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0.002

0

0

0

0

0

0

0

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(<.001)

0

0

0

0

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0

0

0

0

(«) <*) (»)

.04

.05

.002

0

0

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.17

.02

.05

.13

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0

0

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.096

.048

.008

.13

0

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0

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0

0

0

(«)

0

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0

0

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.036

.001

.009

0.001)

.003

.006

0

0

(«)

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0.005

(o. 001)

.001

(8.002)

(«.001)

.001

0

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(«.003)

(0.009)

.002

(8.001)

(0.005)

.001

0

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(8.002)

(o. 001)

(3. 001)

(3.03)

O

.001

.08

.11

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.001

.002

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.21

.04

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(J.005)

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.22

.11

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.24

.001

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.001

.002

.003

.001

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.016

.003

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0

(8.001)

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.59

.12

.013

.040

.005

.015

.020

(». 016)

(3.001)

.005

.036

0.003

0

0

0

0

.001

0

.001

.01

0

0

.001

0

0

0

0

.004

0

0

0

0< ) («) («)

.06

.08

.004

.001

0

.001

.19

.03

.07

.16

.004

0

.007

.046

.030

.16

.080

.021

.19

0

.021

0

.001

.001

0

.001

.009

.001

.012

0

0

.010

.033

.071

.005

.021

.001

.007

.011

0

0

(«)

.020

7-3510

7-3658

7-3490

(7-3488)

7-3495

(7-3488)

(7-3488)

7-3658

(7-3498)

7-3470

(8-0226)

8-0235

(7-3517)

7-3535,7-3720

7-3520

7-3495, 7-3520

7-3520

7-3650

(7-3488)

7-3520

7-3520

7-3520

7-3520

7-3520

7-3598

7-3598

7-3598

7-3598

7-3405

7-3598

7-3698

7-3698

7-3598

7-3658

7-3658

7-3635

7-3630

7-3630

7-3630

7-3630

7-3630

7-3630

7-3658

7-3625

7-3658

7-3635

See footnotes at end of table.
G12 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

TABLE 2. Low-flow characteristics of streams in the study area Continued

Station Station name

Class of stationDrainage 

area 

(sqmi)

Annual low flow, in cubic feet per second per 

square mile, for indicated period of consecutive days and for indicated recurrence interval, 

in years

7-day

2-yr 10-yr

30-day

2-yr 10-yr

Flow, in cubic feet 

per second per square 

mile, which was 

equaled or exceeded 

for indicated percent 

of time

90 95

Daily-record 

station with 

which partialrecord station 

is correlated '

Part 7. Lower Mississippi River basin Continued

7-3641.7..... ..

3642.5.. __

3643- 

3645 ___ -

3646 __ . _

3647.... .

3647.5 . 

3648. _ 

3649 ____

3650 ____

3651. ___ .

3653 . 

3655..... 

3658. 

3658.5 

3659. _

3660 

3661.... 

3662 

3663.5. 

3664 

3673. __ 

3675- 

3680. 

3685.. 

3685.2.... ...

3685.4 

3685.6. ......

3687.5 

afion

3692....- ...

3695 

3700 

3702.. ......

3704.. 

3705. 

3706- _

3708.2- .....

3709.3- 

3710 

3710.5 

3715 

3718. 

3720 . 

Ouachita River basin Continued

Chemin-a-Haut Creek near Berlin, Ark 

Chemin-a-Haut Bayou (Creek) near Beekman, La. 

Bayou Bartholomew near Beekman, La 

Bayou de Loutre near El Dorado, Ark ....

Middle Fork Bayou D'Arbonne near Colquitt, La. 

Middle Fork Bayou D'Arbonne near Bernice, La. 

Cornie Bayou near Three Creeks, Ark..,. 

Little Corney Bayou near Summerfleld, 

La.

Little Cornie Bayou near Junction City, 

Ark.

North Cheniere Creek at Cheniere, La 

Cheniere Creek near BawcomvUle, La._ ..

Big Colewa Bayou near Oak Grove, La ... 

Big Creek at Holly Ridge, La.... ____ .

Bayou La Fourche near Crew Lake, La...

Bills Creek near Mount Pleasant, La ......

Bayou Beaucoup near Cotton Plant, La 

Dugdemona River near Quitman, La _ ..

Dugdemona River near Jonesboro, La _ .

Dugdemona River near Winnfield, La .....

P 

P 

P

D 

P

P 

P 

P 

P 

D

P 

P

D

D 

P

P 

D 

P

P 

P

P 

P 

P 

D 

D

P 

P 

P 

P 

D

P 

D 

D 

P 

P

D 

P 

P 

P 

D

P 

D 

P 

D

88.4 

216 

271

1,645 

78.4

141 

302 

30.0 

68.9 

355

63.3 

43.9

178

180 

54.0

46 

462 

98.2

208 

29.0

87.5 

38 

134 

1,226 

42

71 

347 

25.1 

22.9 

361

101 

309

782 

60 

24.7

271 

127 

117 

46.0 

2.14

19.5 

347 

81 

654

0 

0 

.002

.063 (6)

.06 

.03

(2. 002) 

(2. 02)

(2. 01)

.001

(2. 001)

(2.006)

.002 

.003

.014 

.003 (6)

.002 

(2.01)

.03 

.02 

0 

.05 

0

.008 

.06 

0 

0 

.01

.002 

.03 

.12 

.001

(2.001)

(2 .01) 

(2 . 007) 

.010 

(2.006) 

.07

.09 

.01 

.001 

.005

0 

0 

0

.03 

( >

.03

1

0 

0

0 

0

0 

.001 < >

.010 

0

(6)

0 

0

(6)

.006 (6)

.03 

0

(6) 

.03 (6) 

0 

.003

.001 

.01 

.07 (6) 

0

0 

0 

.002 

0 

.006

.01 

.005 (?

0 

0 

.002

.07 (6)

.08 

.04 

(2.02) 

(2.03) 

.001

.003

(2.01)

.001

.003 

.005

.016 

.007 

.012

.006 

(2. 02)

.03 

.03 

.001 

.06 

0.01)

.008 

.07 (6)

(2 . 001)

.02

.003 

.04 

.15 

.002 

(2.002)

.001) 

(2 .01) 

.016 

(2.02) 

.10

.11

.02 

.001 

.009

0 

0 

.001

.04 (6)

.04 (6) 

0 

0 

0

0

(6)

0 

.001 (6)

.011 

0

(6)

0 

0

(«)

.008 (6)

.03 

0

m. M

(6) 

0 

.004

.002 

.01 

.08 (6) 

0

0 

0 

.003 

0 

.02

.03 

.007 (6) 

.001

(30.008) 

0 

.002

.07 (6)

.08 

.03 

0 

(». 01) 

.001

.003 

(3.06)

(s. 003)

.005 

.004

.020 

.006 

.018

.006 

(«. 005)

.03 

.03 

.001 

.06 

0

(6) 

.07 

«

(3.001)

.02

.003 

.03 

.14 

.002 

(6.002)

.001 

(«.004) 

.015 

(8.006) 

.09

.10 

.02 

.001 

.008

0 

0 

.001

.05 

W

.06 

«

w

0 

0

.001 

0

0

.002 (6)

.014 

.003 (6)

.003 

0

(6) 

.02 (6) 

.05 

0

<«> 

.05 

« 

0 

.01

.003 

.02 

.11 

0 

0

0 (6) 

.009 

0 

.05

.06 

.01 

.001 

.004

7-3658 

(7-3643) 

7-3680

7-3658

7-3635 

7-3647 

(7-3662) 

7-3650

7-3520 

(7-3662)

(7-3647) 

7-3658

7-3658

7-3635 

7-3705

7-3650, 7-3705 

(7-3662) 

7-3705

7-3685 

7-3680

(7-3643)

7-3680, 7-3695

7-3705 

7-3705

7-3720 

7-3720 

7-3520

7-3710

7-3715, 7-3720

Part 8. Western Gulf of Mexico basins

8-0225 ........

Sabine River basin

D 4,858 0.015 0.005 0.021 0.005 0.018 0.010

1 Station numbers shown in parentheses are partial-record stations.

2 Figure is for 1.2-yr recurrence interval; 2-yr figure is 0.

* Figure is for 70 percent of time; figures for 80 percent and 90 percent are 0;

The low-flow data in table 2 are presented in cubic 

feet per second per square mile to facilitate comparison 

of flows of streams with different size drainage areas. 

It should not be inferred, however, that the yield is uniform throughout a drainage basin. On the contrary, 

the low-flow yields usually differ between tributary 

streams within a drainage basin and within reaches on

* Figure is for 5-yr recurrence interval; 10-yr figure is 0. 

» Figure is for 80 percent of time; figure for 90 percent is 0.

 Relation curve not defined in this range.

a single stream. For example, based on use of the 

median annual (2-year) 7-day low flow as the index, the 

low-flow indices for streams in the Saline River basin 

(7-3626 to 7-3629) above the gaging station at Benton, 

Ark. (7-3630), range from 0.005 to 0.071 cfs per sq mi 

(cubic foot per second per square mile). It can also be 

seen that streams having smaller drainage areas may
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G13

have the lower low-flow indices. The differences in 

low-flow indices are primarily due to the difference in 

hydraulic characteristics of the aquifer supplying 

water to the stream, the depth of incision of the stream, 

and the interrelation of the hydraulic characteristics of 

the aquifer and of the stream. The location of the 

stations in table 2 is shown on plate 1. The station 

numbers shown on the plate are the same as those used 

in table 2. The low-flow index (7-day 2-year low flow) 

for each station is given in parenthesis near the station 

symbol. For a few of the stations on the plate a dash 

is shown in the parenthesis, which means that the relation with the daily-discharge station is not defined in 

this range.

LOW-FLOW FREQUENCY

Low-flow frequency data for 50 daily-record gaging 

stations are presented in table 3. Similar data for the 

partial-record stations have not been computed because 

of the limited basic information available at these locations. The data in table 3 can be plotted on graph 

paper similar to that used in figure 3 if a graphical presentation is desired.

4000

1.01 2 10 

RECURRENCE INTERVAL, IN YEARS

50 100

FIGURE 3. Magnitude and frequency of annual low flow for Saline 

River near Eye, Ark., 1929-57.

TABLE 3. Magnitude and frequency of annual low flow at daily-record gaging stations in the study area 

[Data are adjusted to period April 1929-March 1958 on basis of relation to data at other gaging stations]

Station Station name

Drainage 

area 

(sqmi)

Period 

(consecutive days)

Annual low flow, in cubic feet per second, for indicated recurrence interval, in years

1.03 1.2 2 5 10 20 50

Part 7. Lower Mississippi River basin

7-0479.5.... 

0780 _ .....

2645.... .

3395.. ......

8400........

St. Francis River basin 

L'Anguille River at Palestine, Ark ........

White Riser basin

Arkansas Riser basin 

Bayou Meto near Stuttgart, Ark ..........

Red River basin

807

175

560

181

2,674

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

94

154 

245 

385 

790 

1,400

5.7

17 

34 

52 

147 

270

17

36 

62 

160 

420 

590

17

24 

49

74 

158 

272

265

400 

660 

1,100 

2,200 

3,300

23

36 

72 

142 

375 

720

.7

2.3 

8.0 

22

55 

118

.2

2.3 

16

60 

160 

274

2 Q

5.7 

11 

23

80 

162

71

100 

170 

315 

1,140 

2,300

0

.4 

9.4 

42 

143 

295

.1

.4 

1.3 

7.5 

18 

42

0

0 

.6 

13

44 

93

.4

.6 

1.3 

3.6 

16 

65

18

24 

39 

67 

295 

1,080

0

0 

0 

14 

57 

106

0

.1 

.3 

1.9

6.8 

16

0

0 

0 

.6 

9.1 

28

.1

.1 

.1 

.3

3.0 

16

5.0

6.0 

9.1 

15 

61 

320

0

0 

0 

7.2 

36 

60

0

0 

.1

.9 

4.0 

9.2

0

0 

0 

.1 

3.0 

12

0

0 

.1

.1 

.8 

8.6

2.7

3.2 

4.5 

7.3 

32 

190

0

0 

0 

3.6 

24 

35

0

0 

.1

.4 

1.9 

5.7

0

0 

0 

0 

0 

2.3

0

0 

0 

.1 

.3

48

1.6

1.8 

2.5 

3.8 

16 

122

0

0 

0 

.6 

13

18

0

0 

0 

.2 

.7 

3.2

0

0 

0 

0 

0 

.2

0

0 

0 

0 

.1 

1.8

.8

1.0 

1.3 

1.9

7.3 

75

7»3-634^-66 3
G14 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

TABLE 3. Magnitude and frequency of annual low flow at daily-record gaging stations in the study area Continued

Station Station name

Drainage 

area 

(sqmi)

Period 

(consecutive days)

Annual low flow, in cubic feet per second, for indicated recurrence interval, in years

1.03 1.2 2 5 10 20 50

Part 7. Lower Mississippi River basin Continued

7-3405.. ......

3410 __

3425.. ......

3430- 

3435 

3440 

3445.. .

3450 

3460 

3470 

3475.. ......

3480..... _

3490 

Red River basin Continued

361

124

KO7

276

404

2,774

366

79

850

116

364

3,137

1,097

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

52

69 

150 

220 

370 

570

10

14 

35 

56 

111 

188

9 7

4.9 

33 

87 

205 

510

3.4

6.8 

15 

33 

103 

180

9 7

4.1 

27 

85 

275 

610

26

35 

136 

430 

1,500 

3,300

19

22 

36 

66 

148 

385

1 0

2.7 

5.1 

10 

29 

96

44

51 

84 

143 

330 

840

7.8

8.9 

11 

17 

34

77

915

33 

46 

80 

159 

311

65

101 

210 

550 

1,390 

2,920

42

53

70 

140 

420 

810

19

25 

39 

68 

200 

370

2.0

3.9

6.8 

14 

48 

103

0

.1 

.6 

4.2 

62 

170

0

.1 

1.1 

5.0 

26 

90

.8

1.0 

3.1 

15 

83 

210

8.9

12 

31 

85 

380 

1,080

6.5

8.4 

13 

21 

48 

128

.1

.2 

.6 

2.4 

7.0 

23

16

20 

30

49 

108 

280

4.6

5.2 

6.3 

9.2 

17 

34

19

14 

18 

29 

54 

112

25

32 

52 

129 

345 

900

8.8

11 

15

32 

104 

275

7.0

9.1 

11 

17 

49 

155

.1

.2 

.3 

1.4 

9.4 

40

0

0 

0 

0 

3.4 

44

0

0 

0 

.5 

3.5 

26

.4

.5 

.7 

1.9 

15 

55

1.7

2.4 

5.6 

19 

86 

284

.7

1.1 

2.3 

5.1 

13 

32

0

0 

0 

0 

.6

4.4

4.2

5.2 

6.9 

12 

30 

76

2.7

3.0 

3.5 

4.8 

7.8 

14

5.8

6.6 

8.1 

11 

17 

34

11

13 

16

26 

62 

201

1.1

1.3

1.9 

4.0 

15 

61

2.9

3.6 

4.6 

6.9 

15 

46

0

0 

0 

.1 

.9 

10

0

0 

0 

0 

0 

12

0

0 

0 

.1

.5 

3.9

.1

.2 

.2 

.4 

1.4 

14

.1

.2 

.4 

1.2 

16 

83

0

0 

0 

.2 

3.0 

9.5

0

0 

0 

0 

0 

.3

.7

.9 

1.3

2.5 

7.8 

22

2.0

2.2 

2.5 

3.1 

4.6 

7.3

3.7

4.2 

4.9 

5.9

7.8 

12

6.6

7.4 

8.5 

11 

17 

44

.2

.2 

.3 

.5 

2.1 

12

1.8

2.2 

3.0 

4.6 

9.2 

25

0

0 

0 

0

.2 

3.5

0

0 

0 

0 

0 

6.0

0

0 

0 

0

.2 

1.8

0

.1 

.1 

.1

.4 

4.5

0

0 

0 

.1 

1.9 

39

0

0 

0 

0 

.4 

4.9

0

0 

0 

0 

0 

0

.1

.2 

.3 

.8 

3.3 

12

1.8

2.0 

2.2 

2.8 

3.9 

5.6

3.2

3.6

4.2 

4.8 

5.9 

8.4

6 C

6.2 

6.8 

7.9 

11

22

.1

.1 

.1

.2 

.7 

4.6

1.2

1.5

2.1 

3.2 

6.6 

16

0

0 

0 

0 

.1 

1.1

0

0 

0 

0 

0 

3.2

0

0 

0 

0 

.1 

1.0

0

0 

0 

0 

.2 

1.3

0

0 

0 

0 

.2 

16

0

0 

0 

0 

0

2.2

0

0 

0 

0 

0 

0

0

0 

0

.1

1.3

6.8

1.6

1.8 

2.0 

2.5 

3.4 

4.8

9 0

3.2 

3.7 

4.2 

4.9 

6.4

4.6

5.2 

5.7 

6.6 

8.8 

14

0

0 

0 

.1 

.3 

2.1

0.7

.9 

1.4

2.2 

4.6 

9.3

0

0 

0 

0 

0

.2

0

0 

0 

0 

0 

1.5

0

0 

0 

0 

0

.5

0

0 

0 

0.1

.6 

0

0 

0 

0 

0 

4.1

0

0 

0 

0 

0 

.3

0

0 

0 

0 

0 

0

0

0 

0 

0 

.2 

3.2

1.4

1.5 

1.7 

2.2 

2.9 

4.1

9 i

2.7 

3.1 

3.5 

4.1

4.8

3.7

4.2 

4.5 

5.2 

7.0 

10

0

0 

0 

0 

.1 

.8
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G15 

TABLE 3. Magnitude and frequency of annual low flow at daily-record gaging stations in the study area Continued

Station Station name

Drainage

area 

(sqmi)

Period 

(consecutive days)

Annual low flow, in cubic feet per second, for indicated recurrence interval, in years

1.03 1.2 2 5 10 20 50

Part 7. Lower Mississippi River basin Continued

7-3495... __ .

3496.5. __ .

3500... __ .

3510.. ......

3515.. __ .

3515.5. .....

3520... .....

3525... .....

3530-- 

560- 

3598 

3608... 

3610. ..... ..

Red River basin Continued

Ouachita River basin

Ark.

Ark.

546

683

2,628

' 7Q

66

266

154

423

1,386

410

121

380

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7.4

11 

19 

60

225 

550

25

35 

51 

101 

258 

500

133

166 

247 

500 

1,160 

2,600

.7

1.0 

1.9 

3.9 

15 

37

.5

.7 

1.8 

6.5 

28 

58

3.5

6.0 

10 

30 

97 

219

28

30 

32 

42 

86 

139

52

58 

66 

96 

215 

420

136

210 

318 

515 

930 

1,500

67

85 

119 

184 

414 

680

72

87 

114 

150 

317 

560

4.3

6.7 

22 

34 

87 

163

55

69 

100 

165 

390 

600

1.8

2.5 

4.4 

13 

52 

172

4.0

5.7 

8.4 

20 

64 

, 178

58

70 

99 

173 

400 

950

.1

.1 

.4 

.8 

3.1 

10

.1

.1

.2 

.8 

3.3 

14

.2

.4 

.8 

3.3 

20 

68

18

20 

21

27 

44 

68

27

30

34 

48 

98 

184

40

60 

90 

162 

360 

730

34

41 

55 

85 

198 

362

42

46 

58 

81 

152 

280

1.0

1.4 

2.9 

7.3 

33 

76

20

26 

38 

62 

160 

315

0.4

.5 

.8 

2.0 

6.9 

36

.2

.3

.6 

1.6 

8.8 

42

18

22 

29 

44 

100 

263

0

0 

0 

.1 

.3

1.7

0

0 

0 

0 

.2 

1.9

0

0 

0 

.1 

.8 

8.3

11

12 

13 

16 

22 

33

15

16 

18 

22 

39 

70

6.8

10 

16 

32 

95 

270

16

21 

26 

37 

72 

189

24

27 

32 

40 

66 

125

0

0 

.1

.8 

4.3 

22

7.5

9.2 

12 

19 

49 

130

0.2

.2 

.3 

.6 

1.6 

6.3

0

0 

0 

0 

.7 

6.9

5.2

6.1 

7.8 

11 

23 

71

0

0 

0 

0 

0 

.3

0

0 

0 

0 

0 

.2

0

0 

0 

0 

0 

.3

6.8

7.2 

7.9 

9.3 

13 

20

8.8

9.6 

10 

12 

18 

31

.8

1.3 

1.9

4.5 

19 

79

8.4

10 

13 

18 

34 

88

16

17 

20 

23 

36 

62

0

0 

0 

0 

.6 

3.5

4.1

4.9 

6.4 

9.3 

18 

52

0.1

.2 

.2 

.4 

1.0 

3.1

0

0 

0 

0 

.1 

2.0

2.5

2.9 

3.6 

5.1 

11 

38

0

0 

0 

0 

0 

.1

0

0 

0 

0 

0 

0

0

0 

0 

0 

0 

0

5.4

5.8 

6.2 

7.1 

9.7 

16

6.8

7.3 

8.0 

9.3 

13 

22

.2

.3 

.5 

1.2 

6.6 

37

5.6

6.7 

8.4 

11 

24 

58

12

13 

15

18 

28 

44

0

0 

0 

0 

0 

1.5

3.0

3.5

4.7 

6.6 

13 

30

0.1

.1 

.2 

.3

.8 

2.0

0.

0 

0 

0 

0 

.6

1.4

1.6 

2.0 

2.8 

6.0

24

0

0 

0 

0 

0

.1

0

0 

0 

0 

0 

0

0

0 

0 

0 

0 

0

4.3

16 

5.0 

5.7 

7.8 

13

5.4

5.8 

6.4 

7.2 

10 

17

.1

.1 

.1

.4 

2.4 

19

3.8

4.5 

5.6 

7.5 

18 

41

9.5

11 

12

14 

22 

34

0

0 

0 

0 

0 

.6

1.7

2.1 

3.3

4.8 

9.7 

21

0.1

.1

.1 

.2 

.5 

1.2

0

0 

0 

0 

0 

.1

.9

1.0 

1.2 

1.5 

3.3

14

0

0 

0 

0 

0 

0

0

0 

0 

0 

0 

0

0

0 

0 

0 

0 

0

3.2

3.4

3.8 

4.2 

5.8 

9.8

4.0

4.3 

4.7 

5.2 

7.3 

12

0

0 

0 

.1 

.6 

8.6

2.3

2.7 

3.4 

4.5 

12 

29

7.3

8.1 

9.2 

11 

16 

26

0

0 

0 

0 

0 

0

1.1

1.3 

1.6 

2.2 

6.5 

14
G16 WATER EESOUKCES OF THE MISSISSIPPI EMBAYMENT

TABLE 3. Magnitude and frequency of annual low flow at daily-record gaging stations in the study area Continued

Station Station name

Drainage

area 

(sqmi)

Period 

(consecutive days)

Annual low flow, in cubic feet per second, for indicated recurrence interval, in years

1.03 1.2 2 5 10 20 50

Part 7. Lower Mississippi River basin Continued

7-3615........

3625..... 

3630.... .

3635.... ....

3645........

3650.... __

3655 ........

3658 _ .. ...

3660 ........

3680. .......

3685. .......

3690 ........

3695........

Ouachita River basin Continued

Bernice, La.

iai

91ft

569

9 (Ifi9

i ft4<;

180

4.R9

1,226

42

309

7

15 

30 

60 

120

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15

30 

60 

120 

183

7

15 

30 

60 

120 

183

6.5

9.9 

16 

26 

99 

270

0

0 

.7 

2.6 

24 

162

fi9

83 

121 

189 

399 

710

 loo

177 

256 

406 

1,170 

2,270

247

278 

339 

490 

943 

1,660

OO

28 

36 

68 

168 

323

A O

9.2 

12 

26 

74 

156

4.7

5.9 

10 

20 

53 

132

OQ

31 

41 

66

127 

229

199

134 

171 

238 

420 

660

.7

1.2 

2.6 

6.1 

15 

46

QQ

52 

93 

184 

435 

905

27

32 

46 

82 

202 

373

1.5

2.2 

4.2 

8.6 

29 

79

0

0 

0 

.2

2.8 

45

99

34 

48 

75 

194 

372

>>ft

70 

101 

161 

428 

960

160

174 

200 

260 

459 

770

4.7

6.3 

8.7 

18 

50 

125

1.1

1.5 

2.0

5.4 

20 

54

1.2

1.6 

2.6 

7.8 

18 

44

7.6

11 

14 

25 

51 

100

87

94 

112 

139 

216 

320

.1

.1

.4 

1.3 

4.6 

19

14

18 

27 

46 

120 

275

15

18 

23 

33 

68 

129

0.1

.2 

.4 

1.1 

5.3 

19

0

0 

0 

0 

.1 

7.3

19

15 

20 

28 

65 

153

26

30 

39 

56 

133 

329

103

110 

121 

144 

211 

330

.1

.2 

.5 

2.5 

9.9 

34

0

0 

.1

.5 

3.0 

12

.4 

.5 

2.3 

5.3 

13

1.4

2.2 

3.3 

6.4 

14 

33

60

64 

69 

78 

105 

148

0

0 

0 

.1 

.6 

5.3

4.7

5.7 

7.1 

10 

25 

62

8.2

9.2 

11 

13

21 

40

0.1

.1 

.1

.1

.7 

4.9

0

0 

0 

0 

0 

.6

5.3

6.8 

9.0 

11 

26 

55

10

15 

18 

25 

50 

115

70

75 

80 

90 

123 

179

0

0 

0 

.2 

1.5 

7.3

0

0 

0 

0 

.3 

1.8

.1

.1

.2 

.7 

1.8 

5.0

.1

.2 

.5 

1.2 

3.0 

10

44

46 

48 

53 

64

87

0

0 

0 

0 

0 

1.0

1 Q

2.2 

2.6 

3.2 

6.0 

14

5.0

5.4 

6.0 

6.7 

9.4 

16

0

0 

.1 

.1

.2 

1.8

0

0 

0 

0 

0 

0

2 7

3.6 

5.0 

6.9 

18 

35

9 n

10 

12 

17 

34 

71

KT

62 

66 

71 

96 

143

0

0 

0 

0 

.5

2.8

0

0 

0 

0 

.1

.6

.1

.1 

.1

.5 

1.0 

3.0

0

0 

.1 

.3 

1.1

5.0

38

40 

42 

44 

52 

68

0

0 

0 

0 

0 

.3

1 9

1.4 

1.6 

2.0 

3.1 

7.0

3.9

4.2 

4.5 

5.0 

6.6 

11

0

0 

0 

0

.1

.5 

0

0 

0 

0 

0 

0

1.4

1.9 

2.7 

4.5 

12 

24

6.6

7.7 

9.0 

12 

24 

49

4.Q

52 

55 

60 

80 

116

0

0 

0 

0 

.2 

1.2

0

0 

0 

0 

0 

.2

0

0 

.1 

.3 

.7 

1.9

0

0 

0 

.1 

.4

2.7

35

36 

37 

40 

44

57

0

0 

0 

0 

0 

.1

g

1.0 1.1

1.4 

1.9 

4.0

3.3

3.5 

3.7 

4.1 

5.0

7.6

0

0 

0 

0

.1

.2 

0

0 

0 

0 

0 

0

.6

.8 

1.2 

1.9 

6.8 

15

4.5

5.2 

6.0 

7.7 

16 

30

40

42 

44 

48 

62 

88

0

0 

0 

0 

.1 

.4

0

0 

0 

0 

0 

.1

0

0 

0 

.2 

.4 

1.2

0

0 

0 

0 

.1 

1.1

31

32 

33 

34 

38 

46

0

0 

0 

0 

0 

0

.6

.7 

.8 

.9 

1.2 

2.2

2.8

2.9 

3.1 

3.4 

3.8 

5.4
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G17 

TABLE 3. Magnitude and frequency of annual low flow at daily-record gaging stations in the study area Continued

Station Station name

Drainage 

area 

(sqmi)

Period 

(consecutive days)

Annual low flow, in cubic feet per second, for indicated recurrence interval, in years

1.03 1.2 2 5 10 20 50

Part 7. Lower Mississippi River basin Continued

7-3700 . 

3705 

3710-.. 

3715. 

3720..-. 

Ouachita Riser basin Continued

Castor Creek near Grayson, La ______

7(29

271

914.

347

654

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

7

15 

30 

60 

120 

183

ooq

249 

312 

418 

690 

1,110

9.0

11 

13 

25 

63 

133

.6

.6 

.7 

.9 

2.5 

10

1ft

24 

34

74 

187 

380

28

38 

57 

153 

396 

725

1 ^9

168 

194 

243 

372 

535

2.7

3.4 

4.3 

9.3 

23 

60

.3

.4 

.4 

.6 

1.1 

3.6

8.5

11 

14

25 

54 

117

9 Q

13 

19 

39 

99 

235

98

107 

117 

136 

188 

263

.1

.1 

.2 

1.4 

4.1 

18

.2

.2 

.2 

.3 

.5 

1.2

4.3

5.2 

6.4 

9.1 

15 

30

3.1

4.0 

5.7 

10 

18 

48

65

70 

75 

84 

108 

151

0

0 

0 

0 

.1 

3.8

0

.1 

.1 

.1

.2 

.5

2.5

2.9 

3.5 

4.4 

5.8 

9.0

.8

1.1 

1.5 

3.0 

5.3 

11

54

57 

61 

66 

82 

116

0

0 

0 

0 

0 

1.0

0

0.1 .1 .1

.4 

1.8

2.1 

2.5 

3.1

4.0 

5.7

.3

.4

.6 

1.4 

2.7 

5.3

48

50 

53 

57 

67 

92

0

0

0 

0 

0 

.2

0

0 

0 

0.1

.2 

1.3

1.5 

1.8 

2.2 

2.8 

4.1

.1

.1

.2 

,7 

1.5 

3.0

40

42 

45 

47 

54 

71

0

0 

0 

0 

0 

0

0

0 

0 

0

.1

.2

.8

1.0 

1.2 

1.5 

1.9 

2.6

0

0 

.1 

.3 

.8 

1.5

Part 8. Western Gulf of Mexico basins

8-0225- _ . 

Sabine River basin

4,858 7

15 

30 

60 

120 

183

372

433 

619 

1,030 

2,190 

4,060

183

209 

278 

424 

798 

1,650

74

84 

103 

140 

233 

551

32

35 

39

49 

75 

207

22

24 

26 

31 

46 

136

17

18 

20 

23 

35 

94

13

14 

15 

17

26 

58

In table 3, the probability of occurrence is given in 

terms of the average time interval between indicated 

low flows. For example, the lowest average discharge 

for 7 consecutive days on the Saline River near Rye, 

Ark. (7-3635), may be equal to or less than 13 cf s (cubic 

feet per second) at average intervals of 5 years on a 

long-term basis. The chance of occurrence in 1 year 

is 1 in 5, or 20 percent. These recurrence intervals are 

averages and do not imply any regularity of recurrence. 

During the period of record, 1938-57, the 7-day minimum flow near Rye was less than 13 cfs (the 5-year 

event) in 1938,1943,1954, and 1956. Thus, during the 

20-year period, the 5-year event occurred four times; 

this recurrence is in agreement with the probable frequency. The intervals between these occurrences, however, which are 5, 11, and 2 years, demonstrate that 

there was not a regularity of recurrence.

The data in table 3 can be used to estimate the probable future magnitude and frequency of low flows at 

the indicated locations, if it is assumed that the climatological conditions experienced during the reference 

period 1929-57 will not change materially, and provided also that the effects of manmade changes are considered in making the estimates.

FLOW DURATION

Flow-duration data for the 50 daily-record gaging 

stations are presented in table 4. Just as for the lowflow frequency data, flow-duration data are not shown 

for the partial-record stations. The data in table 4 can 

be plotted on logarithmic-probability paper similar to 

that used in figure 4, if a graphical presentation is 

desired.
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,

Sabine Riverat Logansport, La 
G20 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

50,000

10.000

1000

100

0.01 1 50 99,9

PERCENTAGE OF TIME INDICATED DISCHARGE 

WAS EQUALED OR EXCEEDED

FIGURE 4. Flow-duration curves for Saline River near Rye, Ark. 

(drainage area, 2,062 sq mi), and Bayou Bartholomew near Beekman, La. (drainage area, 1,645 sq mi), 1929-57.

The slope of the duration curve is determined by the 

hydrologic and geologic characteristics of the river basin 

upstream from the station, and the slope of the curve 

is a quantitative measure of the variability of the 

streamflow. The slopes of the duration curves for 

streams having large low-flow yields are flatter than 

those for streams having small low-flow yields. For 

example, the duration curve for Bayou Bartholomew 

near Beekman, La. (fig. 4), shows a much lower variability and a higher low-flow yield per square mile than 

does the duration curve for Saline River near Eye, Ark. 

Thus, the flow-duration data in table 4 are excellent 

for comparing the flow characteristics of different 

streams and may be used for preliminary planning, but 

detailed studies will require further analysis and use of 

the low-flow frequency data shown in table 3.

The flow-duration data in table 4 are for the complete reference period, 1929-57; the flow-duration data 

for any particular year can deviate from the data in 

table 4=. For example, during 1943, a year of extremely 

low flow on Black Lake Bayou near Castor, La.

(7-3525), the daily discharge equaled or exceeded 43 cfs 

only 52 percent of the time, whereas during the reference period, the discharge equaled or exceed 42 cfs 70 

percent of the time.

The adjusted data in table 4 can be used to predict the 

long-term distribution of future flows at the indicated 

locations, if it is assumed that the climatological conditions experienced during the reference period, 1929-57, 

will not change materially, and provided that the effects 

of manmade changes are also considered in the 

computation.

FACTORS AFFECTING LOW FLOW

Water that sustains the flow of streams during long 

periods of no precipitation comes from prior precipitation that has been temporarily diverted. Inasmuch 

as the natural diversion of this water is through temporary storage in the geologic units, the low flows of 

streams is governed by the release of the stored water. 

The ability of geologic units to release water from 

storage depends on their composition, and the movement of water through the units depends on their hydrologic character and the hydraulic gradient. The 

principal natural factors influencing the base flow of 

streams are: (1) permeability and porosity of the geologic units, (2) interrelation of the water surface in the 

streams to the elevation of the water table and to the 

base of the aquifers, (3) slope of the water table, and 

(4) rate of evapotranspiration.

The low flows of some of the streams described in this 

report may have been altered from their natural flows 

by manmade practices. Heavy pumping of ground 

water near the stream, for example, may lower the water 

table and permit the stream to yield some of its flow 

to adjacent aquifers, and the dredging of stream channels may increase or decrease the natural low flows of 

the stream. In addition, water is withdrawn from 

the streams for irrigation in many sections of the study 

area. The effect of these manmade changes limits the 

interpretation than can be made of the relation between 

geologic units and the low flow of the streams.

It is not possible to say generally that, in an area 

where one stream shows an index of a given unit yield, 

all streams in the area have the same index. Generally, 

the index differs from stream to stream and may differ 

at different locations on the same stream. The indices 

are the same only where the physical characteristics of 

the factors affecting the low flow are the same. However, the index does provide a means of comparing the 

yield of different areas and provides a basis for study 

of the factors affecting low flow.
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G21

The low-flow characteristics of the streams are compared by using the 7-day low flow for the 2-year recurrence interval, shown in table 2, as an index of low flow. 

The discharge for this median annual 7-day low flow 

is expressed in cubic feet per second per square mile to 

minimize the effect of size of drainage areas and thus to 

emphasize the effects of basin geology.

A study of the data in table 2 indicates large differences in the low-flow yields of the streams in the area, 

which can be attributed to the basin geology. The most 

noticeable differences in low-flow yields are between 

streams that head in the mountains and foothills outside the embayment and those that head in the embayment. The mountains and foothills outside the 

embayment are underlain by Paleozoic rocks which collectively constitute the major contributor to the low 

flow of the streams in the embayment. Streams in the 

Paleozoic rocks that are incised to sufficient depth to 

intercept the ground water have high low-flow indices. 

As these streams enter the embayment, they cross outcrops of Cretaceous and Tertiary deposits, and some 

of the streams enter broad alluvial valleys. In this belt 

just inside the boundary of the embayment, many of the 

streams experience decreases in low-flow yield.

Within the embayment, the geologic units that contribute appreciable water to the low flow of the streams 

are: the alluvium and the sand units in the Claiborne 

Group the Carrizo Sand and Mount Selman Formation in Texas and the Carrizo Sand and Cane Kiver Formation in Arkansas and Louisiana; the Sparta Sand; 

the Cook Mountain Formation; and the Cockfield Formation. The low-flow indices for streams that derive 

their base flow from the alluvium are generally low, but 

the alluvium is an important contributor to the base flow 

of the embayment streams because it is exposed over 

such a large part of the study area.

ST. FRANCIS BIVEB BASIN

The major part of the St. Francis Kiver basin lies 

north of lat 35° N., which is outside the area covered 

in this chapter. Low flows of the main stem of the St. 

Francis Kiver are not shown because it is regulated by 

reservoirs upstream. Fifteen Mile Bayou, the major 

eastern tributary entering the St. Francis Kiver within 

the study area, has a low-flow index of zero at the gaging station near West Memphis, Ark. (7-0479.2). This 

low value probably is the result of diversions for irrigation in the vicinity of West Memphis. The L'Anguille Kiver, which lies west of Crowleys Kidge and 

cuts through the ridge near its southern end, flows 

through a narrow band of alluvium. Most of its eastern tributaries are in Quarternary terrace deposits. 

Some originate in the loess mantle of Crowleys Kidge

which is underlain by sand and gravel, and where the 

tributaries leave the ridge, they flow across outcrops of 

the Claiborne Group. The low-flow index of zero for 

L'Anguille Kiver near Wynne (7-0479.4) and at Palestine (7-0479.5), Ark., is indicative of the low yield of 

the terrace deposits which predominate west of 

Crowleys Kidge.

WHITE BIVEB BASIN

The White Kiver enters the study area at the mouth 

of Bayou des Arc in Arkansas. Flow in the main stem 

is regulated by numerous reservoirs and diversions upstream. Bayou des Arc (7-0768) and Cypress Bayou 

(7-0768.5), which have low-flow indices of zero, head 

in Paleozoic rocks and, after entering the embayment, 

flow through alluvium and terrace deposits. The base 

flow of these streams probably increases downstream 

(derived from water in the alluvium) from the gaging 

stations, which are near the margin of the embayment.

Wattensaw Bayou near Hazen (7-0769.5) and 

Lagrue Bayou near Stuttgart (7-0780), Ark., which 

have low-flow indices of 0.001 cfs per sq mi, receive 

their base flow almost entirely from Quaternary terrace 

deposits. Small parts of their basins near the White 

Kiver are in the alluvium, and the headwaters of Wattensaw Bayou are in Tertiary sediments. Flow of 

many of the tributaries along the southern reach of the 

White Kiver are affected periodically by diversions for 

irrigation.

The Cache Kiver may be affected by diversions for 

irrigation in the extreme upper part of the basin. At 

Patterson, Ark., which is about 20 miles north of where 

the stream crosses into the study area, the effects from 

irrigation, if any, are less noticeable; the index at 

Patterson is 0.042 cfs per sq mi. The base flow probably 

is derived from the alluvium. Big Creek at Poplar 

Grove (7-0779.5) and its tributary Big Cypress Creek 

at Turner (7-0779.7), which have indices of 0 and 0.001 

cfs per sq mi, respectively, are in Quaternary deposits. 

The low flows of both streams may be affected by 

diversions for irrigation.

ABKANSAS BIVEB BASIN

The Arkansas River enters the embayment at Little 

Kock, Ark. The flow of the main stem is affected by 

diversions and regulated by many reservoirs upstream. 

The effect of this regulation on low flows is not known. 

The Corps of Engineers multipurpose project in the 

Arkansas Kiver basin, now in progress, will have a 

beneficial effect on low flows of the Arkansas River. 

The magnitude of the increase in low flows due to the 

multipurpose project can only be estimated, but a 50- 

percent increase would not be unreasonable, depending
G22 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

upon the operation at the nine flood-control reservoirs 

in eastern Oklahoma and western Arkansas.

The Arkansas Kiver immediately west and south of 

Little Kock is in a very narrow alluvial valley; it has 

no major tributaries in the embayment. The Maumelle 

Kiver, which drains an area of Paleozoic rocks, enters 

the Arkansas River just outside the embayment boundary. Flows in the lower reach of Maumelle Eiver are 

regulated by Lake Maumelle, and the yield of this area 

is unknown. Fourche Creek which flows around the 

southern edge of Little Eock has a low-flow index at 

the gaging station (7-2636) of 0.001 cfs per sq mi, but 

the effect of urban and industrial development in the 

Little Eock area on the low flow of this stream has not 

been determined.

East of Bayou Meto, the Grand Prairie region (fig. 

2) is covered by terrace deposits. Low-flow indices in 

this area are 0.001 cfs per sq mi or less at all the gaging 

stations except Bayou Meto near Lonoke, Ark. (7-2640), 

which has an index of 0.010 cfs per sq mi. Bayou Meto 

near Lonoke is affected by drainage from irrigation and 

from a large minnow farm. Water for irrigation is 

pumped from many shallow wells and is diverted from 

many streams and reservoirs in the Grand Prairie region. The water table in the area has been progressively 

lowering for many years, and in some reaches along the 

Arkansas Eiver, the water table slopes away from the 

river.

OITACHITA RIVER BASIN

The Ouachita Eiver and many of its tributaries head 

in the Ouachita Mountains west of the embayment, and 

at the gaging station near Mount Ida, Ark. (7-3560), 

which is above any known regulation on the Ouachita 

Eiver, the index is 0.039 cfs per sq mi. A series of dams, 

which maintains a year-round navigable depth on the 

main stem of the Ouachita Eiver from Camden, Ark., 

to its mouth, prevents the obtaining of accurate 

low-flow measurements. The low-flow characteristics, 

therefore, are not determined.

The tributary streams entering the Ouachita Eiver 

upstream from the Little Missouri Eiver have indices 

ranging from 0.020 to 0.15 cfs per sq mi. Caddo Eiver 

at Caddo Gap, Ark. (7-3596), which has a low-flow 

index of 0.15 cfs per sq mi, drains an area of Paleozoic 

rocks. The Caddo Eiver between Caddo Gap and Alpine (7-3598), Ark, and Gulpha Creek above the gaging station near Hot Springs, Ark. (7-3587), are also 

in the Paleozoic rocks; the Caddo Eiver in this reach 

has a computed index of 0.037 cfs per sq mi and Gulpha 

Creek has an index of 0.028 cfs per sq mi. L'Eau Frais 

Creek receives its base flow from the lower part of the 

Claiborne Group; at Joan, Ark. (7-3601), the low-flow 

index for this stream is 0.020 cfs per sq mi.

Low-flow indices of the Little Missouri Eiver and 

its tributaries vary considerably. At upper elevations, 

the Little Missouri Eiver basin is in Paleozoic rocks. At 

the gaging station near Langley (7-3602), the index is 

0.19 cfs per sq mi, which is reasonably consistent with 

that for Caddo Eiver at Caddo Gap. Downstream from 

Langley, the Little Missouri flows through the Paleozoic foothills and enters the embayment in a broad alluvial valley as it crosses the outcrop of the Trinity 

Group of the Lower Cretaceous Series. The low flow 

decreases between Langley and the gaging station near 

Murfreesboro, Ark. (7-3610), where the index is 0.020 

ef s per sq mi. The decrease in flow is attributed to loss 

of water into the alluvium.

At the gaging sites on the tributaries, Muddy Fork 

(7-3608), Ozan Creek (7-3612), Antoine Eiver (7- 

3615), Terre Eouge Creek (7-3616.5), Caney Creek (7- 

3617), and Terre Noire Creek (7-3618), the indices are 

0.001 cfs per sq mi or less. Most of these streams head 

in the Paleozoic rocks or in the Tokio Formation of 

the Upper Cretaceous Series. In addition, Terre Eouge 

Caney, and Terre Noire Creeks cross outcrops of the 

Nacatoch Sand of the Upper Cretaceous Series or the 

Wilcox, Claiborne, or Midway Groups of the Paleocene 

and Eocene Series, but the yield from these geologic 

units to these streams is very low.

Below the mouth of the Little Missouri Eiver, tributaries to the Ouachita Eiver from the south side, 

near El Dorado, Ark., which are in the sands and clays 

of the Claiborne Group, generally have higher indices 

than tributaries to the Ouachita from the north side, 

which are mostly in Quaternary terrace deposits. 

Smackover Creek near Smackover (7-3621), which is a 

south-side tributary, has an index of 0.012 cfs per sq mi, 

whereas Tulip Creek (7-3618.5), Bayou Freeo (7-3619), 

Moro Creek (7-3625.5), and Eagle Creek (7-3640.2), 

which are north-side tributaries, have indices that range 

from 0 to 0.009 cfs per sq mi.

The upper tributaries to the Saline Eiver in the northern tip of the Ouachita Eiver basin in Arkansas drain 

Paleozoic rocks. The index of the Middle Fork at 

Crows (7-3627) is 0.033 cfs per sq mi, and the South 

Fork near Hot Springs (7-3628) has an index of 0.071 

cfs per sq mi. Lower indices occur on Alum Fork 

(7-3626), index 0.010 cfs per sq mi, and on North Fork 

(7-3629), index 0.005 cfs per sq mi. As the >Saline 

Eiver leaves the Paleozoic rocks and flows across the embayment, the low-flow indices of the main stem decrease ; at Benton (7-3630), the index is 0.021 cfs per 

sq mi, whereas near Eye (7-3635), it is 0.013 cfs per sq 

mi. Most of the Saline Eiver tributaries within the embayment are in the Midway, Wilcox, and Claiborne 

Groups, and, in addition, Hurricane Creek (7-3633)
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G23

has some exposure to the Paleozoic rocks near the boundary of the embayment. The alluvial valley of the Saline 

River between Benton and Rison crosses the sands and 

clays of the Wilcox and Claiborne Groups, and from 

Rison to Rye it crosses clays of the Jackson Group. The 

Jackson Group is not considered an aquifer, and the 

decrease in low flow between Benton and Rye is not 

unreasonable because the tributaries in this general 

area are low-yielding streams having indices of 0.001 

to 0.007 cfs per sq mi. Hudgin Creek near Pansey, 

Ark. (7-3637), which lies east of the Saline River and 

drains partly from the Quaternary terrace deposits and 

partly from outcrops of the Jackson group, has an index 

of zero.

Bayou Bartholomew, the Boeuf River, the Tensas 

River, and Bayou Macon are eastern tributaries of the 

Ouachita River. Bayou Bartholomew is in an 

abandoned course of the Arkansas River. The main 

stem of Bayou Bartholomew lies in the alluvium from 

near Pine Bluff, Ark., to its mouth. Many of its 

tributaries which enter from the west head either in the 

Jackson Group or in terrace deposits and flow across 

terrace deposits to the alluvial valley of the main stem. 

Tributaries entering from the east are in the alluvium 

or in terrace deposits. The low-flow index of Bayou 

Bartholomew is 0.022 cfs per sq mi near McGehee, Ark. 

(7-3641.5), and at the gaging station near Beekman, 

La. (7-3645), the index is 0.063 cfs per sq mi. The index at McGehee may be affected by diversions for irrigation upstream, which have less effect on the Beekman 

index.

The Boeuf River, Tensas River, and Bayou Macon 

basins are in the alluvium. The Boeuf River basin includes the tributaries, Big Colewa Bayou, Big Creek, 

Bayou La Fourche, and Turkey Creek. The Tensas 

River basin includes the major tributary Bayou Macon 

and a network of small streams, some of which follow 

abandoned channels of the large streams that drained 

the area. Gaging stations in Louisiana on the main 

stems, Boeuf River near Girard (7-3680), Tensas River 

at Tendal (7-3695), and Bayou Macon near Delhi 

(7-3700), have low-flow indices of 0.05, 0.03, and 0.12 

cfs per sq mi, respectively. These stations are on a 

line approximately east-west at lat 32°30' N.; because 

the streams here are cut into aquifers in the basal part 

of the alluvium, they have high low-flow yields.

In the Bouef River basin in Louisiana, Big Creek at 

Holly Ridge (7-3685.2) and at Mangham (7-3685.4), 

has low-flow indices of 0.008 and 0.06 cfs per sq mi, 

respectively. The Mangham station has the higher index because it is farther west than the Holly Ridge 

station where the alluvial deposits are thinner, and it 

is south of the latitude where most of the large streams

are cut into the basal part of the alluvium, which results 

in higher low-flow yields. B ayou La Fourche near Crew 

Lake (7-3690) and Turkey Creek at Winnsboro 

(7-3692), which also are cut into this shallow layer of 

alluvial material, have low-flow indices of 0.01 and 0.002 

cfs per sq mi, respectively. Big Colewa Bayou near 

Oak Grove (7-3685), Little Creek near Mangham 

(7-3685.6), and Bayou Galion near Mer Rouge 

(7-3687.5), all have low-flow indices of zero. This is 

probably due to the streams not being cut deep enough 

into the high-yielding alluvial aquifer.

The western tributaries of the lower Ouachita River 

immediately south of El Dorado, Ark., which have 

low-flow indices ranging from near 0 to 0.06 cfs per sq 

mi, lie in the Claiborne Group or in Quaternary terrace 

deposits underlain by the Claiborne Group.

Bayou de Loutre near Laran, La. (7-3647), which lies 

in the low-yielding Cockfield Formation of the Claiborne Group, has a low-flow index of 0.06 cfs per sq mi. 

The index may be affected by the influent of wastes from 

oil-field operations upstream. The downstream station, at De Loutre, La. (7-3647.5), which has a lower index of 0.03 cfs per sq mi, is in the Cook Mountain 

Formation of the Claiborne Group. The fact the 

drainage area at the gaging station at De Loutre is more 

than twice the drainage area near Laran indicates that 

there is little or no yield to this stream from the Cook 

Mountain Formation.

Bayou D'Arbonne and most of its tributaries (7-3648 

to 7-3663.5) have little or no sustained flow during dry 

periods. Most of the Bayou D'Arbonne basin is in the 

Cook Mountain Formation. Three Creek near Three 

Creeks, Ark. (7-3659), has a low-flow index of 0.014 Cfs 

per sq mi, which may be caused by the influent of oilfield wastes.

The Ouachita River tributary, Cheniere Creek near 

Bawcomville (7-3675), and its tributary, North Cheniere Creek at Cheniere (7-3673), which derive their 

base flow mostly from the alluvium, have low-flow indices of 0 and 0.02 cfs per sq mi, respectively.

Streams in the Castor Creek basin in Louisiana 

(7-3702 to 7-3706) are in the low-yielding Cook 

Mountain and Cockfield Formations and in Quaternary 

terraces. The upstream gaging station, Castor Creek 

at Chatham (7-3702), has a low-flow index of 0.001 cfs 

per sq mi and is the only station in the Castor Creek 

basin that has an index greater than zero. Although 

Castor Creek lies predominantly in the Cook Mountain 

Formation, its probable partial contact with the Sparta 

Sand of the Olaiborne Group may result in some lowflow yield.

Streams in the Dugdemona River basin have higher 

sustained low flows than streams in the Castor Creek
G24 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

basin. Dugdemona River upstream from Jonesboro, 

La., derives its base flow from the Sparta Sand. The 

stream has a low-flow index of 0.01 cfs per sq mi near 

Quitman (7-3708.2) and near Jonesboro (7-3715). 

The reach of the channel between Jonesboro and Winnfield is cut into the alluvium and terrace deposits, and 

the low-flow index near Winnfield (7-3720) is 0.005 cfs 

per sq mi. Two small tributaries, Garrett Creek at 

Jonesboro (7-3710) and Dukedall Creek near Danville 

(7-3710.5), which have low-flow indices of 0.07 and 0.09 

cfs per sq mi, respectively, lie wholly in the Sparta 

Sand. Big Creek near Dodson, La. (7-3718), which 

has an index of 0.001 cfs per sq mi, probably receives 

its small base flow from local terrace deposits.

RED RIVER BASEST

The low flows of the main stem of the Bed Eiver are 

affected by regulation from reservoirs upstream, and 

the low-flow characteristics have not been determined. 

However, the low-flow characteristics of the numerous 

tributaries are indicative of streams within the basin 

in the embayment.

The Little Eiver and its main tributaries from the 

north, which rise outside the embayment, have low-flow 

indices ranging from 0.001 to 0.019 cfs per sq mi. 

Within the embayment, the Little Eiver and its northern tributaries cross Cretaceous outcrops, which contain 

aquifers of the Trinity Group, the Woodbine and 

Tokio Formations, and the Nacatoch Sand. Rolling 

Fork upstream from De Queen, Ark. (7-3395), index 

0.002 cfs per sq mi, and its tributary, Robinson Creek, 

are in Paleozoic rocks; and few small tributaries to 

Rolling Fork flow across the Trinity Group. The 

Cossatot River heads in the Paleozoic rocks, and its 

valley cuts through the Trinity Group and Woodbine 

Formation of the Cretaceous System. Cossatot River 

near De Queen, Ark. (7-3405), index 0.019 cfs per sq mi, 

is fed by many tributaries; in addition, because the total 

length of the Cossatot River system of channels is much 

greater than that of Rolling Fork, the Cossatot River 

has a great opportunity for interception of ground 

water. Saline River upstream from Dierks, Ark. (7- 

3410), which has an index of 0.001 cfs per sq mi, is in 

Paleozoic rocks. Downstream from Dierks, within the 

embayment, the stream cuts through the Trinity Group 

and the Woodbine and Tokio Formations. The index 

on the main stem of Little River near Horatio, Ark. 

(7-3400), is 0.007 cfs per sq mi, which compares favorably with the indices for its tributaries. Tributaries 

from the south downstream from Horatio are in terrace 

deposits.

As the Red River flows through the gently rolling hill 

country of the embayment in Arkansas and Texas, it is

fed by many small tributaries of low yield. Walnut 

Bayou (7-3369), Barkman Creek (7-3369.5), and McKinney Bayou (7-3423.5) all have low-flow indices of 

zero at the gaging sites. They are all near the edge of 

the alluvium. Manice Bayou near Canfield (7-3421.5), 

which has an index of 0.002 cfs per sq mi, is in the 

alluvium.

The western limit of the study area in Texas is long 

94°45' W. The gaging station on the main stem of the 

Sulphur River near Talco, Tex. (7-3432), and those 

on the North Sulphur (7-3430) and South Sulphur 

(7-3425) Rivers near Cooper, Tex., all of which are 

outside of the study area, have low-flow indices of zero. 

Upstream from Talco, the Sulphur River and its tributaries entering from the north are underlain by the 

Navarro Group and by the Taylor Marl of Cretaceous 

age. The South Sulphur River flows through the 

Navarre and the Midway Groups. Whiteoak Creek 

near Talco (7-3435), which has an index of 0.001 cfs 

per sq mi, flows through the Midway Group almost 

parallel to the Sulphur River and a few miles to the 

south of it. Sulphur River tributaries to the north, 

in the vicinity of Texarkana (7-3441 and 7-3443), are 

underlain by the Midway Group and Wilcox Formation 

and have indices of zero.

Cypress Creek lies in the Wilcox Formation and the 

Claiborne Group. It is in an area of slightly higher 

yield in Texas than that of the Sulphur River. Along 

the main stem and tributaries of Cypress Creek, the 

indices range from 0 to 0.005 cfs per sq mi. The index increase of 0.003 cfs per sq mi on the main stem of 

Cypress Creek between Pittsburg (7-3445) and Jefferson (7-3460) may be due to yield from the Claiborne 

Group. Regulation by Lake O' the Pines since 1958 

has completely changed the low-flow regime at Jefferson. The tributaries to the Cypress Creek-Twelvemile 

Bayou basin that enter downstream from Jefferson have 

indices that range from 0 to 0.02 cfs per sq mi. Prewitt 

Creek near Karnack, Tex. (7-3460.8), a southern tributary to Cypress Creek, is underlain by the Reklaw 

Member of the Mount Selman Formation, the Carrizo 

Sand, and the Wilcox Formation, and has an index 

of 0.003 cfs per sq mi. The Black Bayou basin, a tributary to Cypress Creek from the north, lies in the lower 

part of the Claiborne Group and in Quaternary terrace 

deposits upstream from Hosston, La. (7-3465), and has 

low-flow indices of 0.002 to 0.003 cfs per sq mi. Cross 

Bayou, which includes the Paw Paw Bayou drainage, 

lies in the Wilcox Group and Quaternary terrace deposits; Paw Paw Bayou near Greenwood, La. (7-3482), 

has a low-flow index of zero. Kelly Bayou near Hosston 

(7-3470) and the lower reach of Black Bayou in the 

vicinity of Gilliam, La. (7-3475), both of which have
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G25

a low-flow index of 0.02 cfs per sq mi, are in dredged 

channels which cut into the Quaternary alluvium.

Bayou Pierre, a western tributary of the Red River 

in Louisiana, has two gaged tributaries, Boggy Bayou 

(7-3510) and Cypress Bayou (7-3515). These streams, 

both of which have a low-flow index of zero, are in the 

Midway Group. Bayou Na Bonchasse near Mansfield, 

La. (7-3517), in the Bayou Pierre basin, has a low-flow 

index of 0.04 cfs per sq mi; this stream is also in the 

Midway Group, but it is probably incised into sands 

of the Wilcox Group and thus has the higher index. 

The headwater of Bayou Na Bonchasse lies partly in 

the Midway Group, which contributes very little to the 

total yield. Two streams that lie in the Eocene and 

Paleocene Series are Buffalo Bayou near Naborton, La. 

(7-3517.2), and Bayou Terre Blanc near Alien, La. 

(7-3517.6); both streams are cut into the Naborton 

Formation of the Wilcox Group, which is composed of 

calcareous and lignitic sands, silts, and clays. These 

streams have low-flow indices of zero. Rambin Bayou 

near Frierson, La. (7-3516.7), which has a low-flow 

index of zero, lies mostly in Quaternary terraces.

The eastern tributaries to the Red River in Arkansas, 

downstream from the Little River, are in an area of 

low yield that extends south into northern Louisiana. 

In the Loggy Bayou basin, 10 of the 15 gaging locations 

have an index of zero. The streams in the Loggy 

Bayou basin in Louisiana north of about lat 32°30' N. 

lie mostly in Quaternary terrace deposits and are not 

cut deep enough into the geologic units to reach the 

ground-water levels. Black Bayou at Leton, La. 

(7-3487.6), lies principally in the Cook Mountain Formation of the Claiborne Group. Two streams in this 

basin, Bayou Dorcheat near Minden, La. (7-3490), and 

Bodcau Bayou near Sarepta, La. (7-3495), have a lowflow index of 0.001 cfs per sq mi. These streams flow 

out of the Wilcox Group or Claiborne Group and are 

predominantly in Quaternary terrace deposits, but they 

have some contact with the Quaternary alluvium. The 

Quaternary alluvium presumably contributes the baseflow yield. The two streamflow stations south of lat 

32°30' N., Brushy Creek near Sibley (7-3491) and 

Loggy Bayou near Ninoch (7-3500), La., have low-flow 

indices of 0.01 and 0.007 cfs per sq mi, respectively. 

Brushy Creek above the station near Sibley has contact with the Sparta Sand of the Claiborne Group, 

whereas the lower reaches of Loggy Bayou have considerable contact with the Quaternary alluvium.

The low-flow indices of streams in the Saline Bayou 

basin in Louisiana range from 0 to 0.20 cfs per sq mi. 

Streams which derive their base flow from the Sparta 

Sand have indices of 0.07 cfs per sq mi or higher,

whereas streams which derive their base flow from 

Quaternary deposits or the Cook Mountain Formation 

have lower indices. The following are the low-flow 

indices for the streams that derive their base flow from 

the Sparta Sand: Saline Bayou near Lucky (7-3520), 

0.07 cfs per sq mi; Saline Bayou near Goldonna 

(7-3521), 0.09 cfs per sq mi; Kepler Creek near Sparta 

(7-3524), 0.20 cfs per sq mi; and Castor Creek at Castor (7-3527), 0.16 cfs per sq mi. Black Lake Bayou 

near Minden (7-3522) has a low-flow index of 0.004 cfs 

per sq mi, whereas at the downstream gaging station 

near Castor (7-3525), which is in the alluvium and terrace deposits, the low-flow index is 0.03 cfs per sq mi; 

the increase in yield is derived from high-yielding tributaries which are in the Sparta Sand. The lower part 

of the Saline Bayou basin is in the alluvium, and the 

low-flow index near Clarence (7-3530) is only 0.005 cfs 

per sq mi. The decrease in yield between Goldonna 

and Clarence is attributed to the low-yielding tributary 

area and to large evapotranspiration losses in the intervening chain of shallow lakes. Two tributaries in this 

low-yielding area, which have low-flow indices of zero, 

are Black Lake Creek near Gibsland (7-3523), which 

is in the Cook Mountain Formation, and Grand Bayou 

near Coushatta (7-3528), which is in terrace deposits.

MAJOR FLOODS AND GROUND-WATER RECHARGE

Streams may be divided into two general categories 

in relation to ground water: (1) effluent streams which 

receive water from underground sources and (2) influent streams which yield water to underground reservoirs. Effluent streams are more numerous in the 

humid zones, and inffuent streams are characteristic of 

the arid regions. In the Mississippi embayment, most 

of the streams are usually effluent but may become influent during periods of drought. During periods of 

high stage, also, an effluent stream may become influent, 

or at least cease to be effluent, during which time the 

normal ground-water yield is held in storage.

Ground-water recharge during times of floods on 

effluent streams is generally temporary. This water is 

stored during the period of high stage on the river and 

is released soon after the flood recedes.

Along the Arkansas River, a definite relation exists 

between river stage and the elevation of the ground 

water. Typical hydrographs of the Arkansas River 

and of wells near Pine Bluff are shown in figure 5. In 

the Arkansas River valley, this relation becomes less 

detectable as the distance from the river increases, and 

the relation is almost imperceptible at distances of 3 to 

4 miles. Wells 1, 2, and 3 are 2.0 miles, 0.4 mile, and 

0.3 mile, respectively, from the river.
G26 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

o

ifD: 5

U)

o

10

15

20

Well 3 r

25

LJ20 

u

o 

< 10

o: LJ

E 

0

-4

Arkansa

Jan. Feb. Mar. Apr. May June July Aug. Sept. Oct. Nov. Dec.

1958

Jan. Feb. Mar. Apr. May June July Aug. Sept. Oct. Nov. Dec.

1959

FIGURE 5. 'Arkansas River and wells near Pine Bluff, Ark., 1958-59.

As illustrated in figure 5, it is recognized that an 

evaluation of changes in ground-water level should give 

consideration to the effects of changes in river stage. 

Recharge effects may be evident at locations fairly 

remote from the flooded area depending on the characteristics and extent of the aquifers adjacent to the 

stream.

LOW FLOWS AND GROUND-WATER FLUCTUATIONS

In the discussion of factors affecting low flow 

(p. G20), the first factor expresses the influence of the 

fixed physical properties of the aquifer in contact with 

or adjacent to the stream, and the other three are 

variable factors that need to be considered in relating 

the water level in the aquifers to the low flow. Because 

the geologic units are the natural storage reservoirs 

that sustain base flow, fluctuation in the ground-water 

table (or in the water surface in the streams) and the 

resulting variation in the slope of the water table 

toward the stream influence the rate at which the 

aquifer yields water to the stream at low flow. Thus, 

the fluctuations in the base flow of a stream are related

to the fluctuations of the ground water in the geologic 

units from which the stream receives its base flow, and 

the ground-water yield to a stream is represented approximately by the base flow of the stream.

For streams that receive their base flow from a single 

geologic unit, the elevation of the ground water in the 

geologic unit is generally an index of the base flow. 

Very few streams, however, receive their base flow 

from a single geologic unit, and the relation becomes 

extremely complex for the larger streams that may 

receive their base flow from several geologic units. In 

addition, in many parts of the study area, evapotranspiration exerts a seasonal effect on streamflow which is 

difficult to evaluate.

The volume of ground water available to support low 

flow is the volume of water in the aquifers adjacent to 

the stream and at an elevation higher than that of the 

water surface in the stream. The size of the surface 

drainage area, then, is not always a dependable basis 

for appraising the low-flow characteristics of streams, 

because (1) the limits of the ground-water aquifer may 

not coincide with the surface drainage area and (2)
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G27

there is great variation in the characteristics of each 

geologic unit from which the base flow of a stream is 

derived. The variations in the runoff per square mile 

presented in table 2 demonstrate the effect of the underground factors on base flow and provide an index for 

use in further investigation into the physical basis for 

the areal variation in the low-flow yields. In estimating low-flow characteristics, discharge measurements 

of low flow at the site should be available, and consideration should be given to the low-flow characteristics of other streams in similar geologic settings.

METHOD OF STUDY

The method used to analyze basic data and to obtain 

the low-flow frequency and flow-duration data presented in this report is mainly graphical. The procedure consisted of smoothing the low-flow data for 

long-term records by comparison with data from other 

long-term stations, and of then adjusting the shorter 

records to the reference period through their relations 

with the long-term records. Statistical principles were 

used as a guide in evaluating the relations.

The following long-term stations served as a basis 

for the low-flow analyses in southern Arkansas, northern Louisiana, and northeastern Texas:

Station Station name 

7-0375_____ St. Francis River near Patterson, Mo. 

7-0570_____ Buffalo River near Rush, Ark. 

7-3635_____ Saline River near Rye, Ark.

7-3645 Bayou Batholomew near Beekman, La.

8-0135 Calcasieu River near Oberlin, La. 

8-0225 Sabine River at Logansport, La. 

8-0335 Neches River near Rockland, Tex.

Smoothed low-flow frequency curves for these stations 

were taken from a report by Hardison and Martin 

(1963). Flow-duration curves were obtained by drawing smooth curves through the plots of the observed 

data for the reference period and giving some consideration to the shape of the flow-duration curves at other 

long-term stations.

Index stations were selected from the remaining stations having long records to obtain a representative 

distribution over the area. The low-flow records at these 

index stations were related to those at the long-term 

stations and then were used as a base to which to relate 

the flow data at stations having records shorter than 

those at the index stations. Data from daily-record stations having less than 5 years of record and data from 

low-flow partial-record stations were related to the data 

from one of the long-term stations.

The reference period used for this study is the 29- 

year period 1929-57, because this period was the longest 

for which a representative number of records was available at the selected long-term stations and at the index

stations. The annual minimum discharges used in the 

low-flow frequencies are the lowest in each climatic 

year; hence the periods of low flow, which usually occur in the summer and fall, are included in the same 

year. The flow-duration sequences are for complete 

water years.

Low-flow frequency and flow-duration results for partial-record stations and for daily-record stations having only a few years of continuous record are much 

less accurate than are similar results for the longer term 

stations, because the data relate to a smaller range of 

discharge and a smaller variety of experience.

More detailed descriptions of the methods used in the 

study and the analyses of the records are given by iSpeer, 

Golden, Patterson, and others (1964).

BASIC DATA FOR THE ANALYSIS

The basic data for the results presented in this report 

are the records of discharge collected at 50 daily-record 

and 106 partial-record stations in or adjacent to the Mississippi embayment in southern Arkansas, northern 

Louisiana, and northeastern Texas. Location of the 

stations is shown on plate 1. The names of the stations are given in table 2.

Most of the streamflow records used in the analysis 

have been published annually in reports of the Geological Survey; a few were furnished by other agencies. 

The United States is divided into 14 parts to facilitate 

publication of the records. All the records in the area 

covered by this report are in Part 7 (fig. 6), Lower 

Mississippi River basin, except the Sabine River at 

Logansport, La., which is in Part 8, Western Gulf of 

Mexico basins.

Records of daily discharge for gaging stations having five or more complete consecutive water years not 

affected by regulation or diversion were processed by 

an electronic computer to obtain (1) the lowest mean 

discharge occurring during each year for selected numbers of consecutive days and (2) the number of daily 

flows each year between selected limits of discharges 

(Speer, 1960). If the natural flow at a station became 

materially regulated or was affected by diversions as 

the result of manmade changes, the data for the record 

so affected were not used. Records for less than 5 complete years were not processed by electronic computer 

but were analyzed as low-flow partial-record stations.

DRAFT-STORAGE RELATIONS

The discharges given in table 2, 3, and 4 are indications of the natural flow of the streams. Storage must 

be provided for drafts greater than the natural flow. 

The amount of such storage and the frequency with 

which it is required provide a basis for obtaining an
G28 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

KANSAS

38

Area covered by this report

FIGURE 6. Map of Mississippi embayment showing areas covered, by numbered parts, for which streamflow records are published in reports on surface-water supply.

economic balance between the cost of the storage and the 

loss resulting from an insufficient supply at periodic intervals. The low-flow frequency data for the 50 stations in table 3 were used to estimate the draft that may 

be maintained from specified amounts of storage.

To provide a means for estimating the storage required for various drafts at other sites, the storage-required frequency data are related to the median annual 

7-day (7-day 2-year) low flows as shown in figures 7 

and 8. This index of low flow, which is the same as

that used, in the section on "Factors affecting low flow," 

is given in table 2 for 88 sites in the study area. For 

other sites, the index usually can be estimated by making a few measurements of low flow and relating the 

measured discharge to the concurrent discharge at the 

nearest site listed in table 2 at which an acceptable correlation can be obtained (Searcy, 1959, p. 20). Application of frequency data for intermittent streams to 

storage problems is not recommended. At present, 

techniques are not sufficiently well developed to permit
LOW FLOW IN SOUTHERN" ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G29

40 60

STORAGE, IN ACRE-FEET PER SQUARE MILE

A

0.2 0.3 0.4 0.5

MEDIAN ANNUAL 7-DAY LOW FLOW. IN CUBIC FEET PER SECOND 

PER SQUARE MILE

B

FIGURE 7. Areal draft-storage relations for a 10-year recurrence Interval as a function of the median annual 7-day low flow, for storage of 0, 5,15,30, 60, and 90 acre-ft per sq mi.

draft-storage analysis on a frequency basis for streams 

with indices of zero.

Data available to define the curves in figures IB and 

SB in the area covered by this chapter are very limited 

because of the large number of low-flow indices that are 

zero. To improve the reliability of the curves, similar 

data for the embayment in northern Arkansas and Missouri are included, and a single set of curves is developed 

for the Mississippi embayment in Arkansas, Missouri, 

northern Louisiana, and northeastern Texas. The number of points available to define the curves ranges from 

4 for the 90 acre-ft per sq mi (acre-feet per square mile) 

at the 20-year recurrence interval to 66 for 0 acre-ft per

40 60

STORAGE. IN ACRE-FEET PER SQUARE MILE

A

MEDIAN ANNUAL 7-DAY LOW FLOW, IN CUBIC FEET PER SECOND 

PER SQUARE MILE

FIGURE 8. Areal draft-storage relations for a 20-year recurrence interval as a function of the median annual 7-day low flow, for storage of 0, 5, 15, 30, 60, and 90 acre-ft per sq mi.

sq mi at the 10- and 20-year recurrence intervals and 

for 5 acre-ft per sq mi at the 10-year recurrence interval. 

The scatter of the circles in figure IB for a storage of 

15 acre-ft per sq mi is typical of the scatter of the points 

that define other curves in the two lower graphs. The 

curves in figures TA and 8A are based on the curves in 

IB and 8B.

The curves of zero storage in figures 7 and 8 represent the 7-day low flow for the 10-year or 20-year 

recurrence interval and thus neglect the small amount 

of storage that will be required to regulate the 7-day 

flow within the minimum. None of the curves include 

reservoir losses or losses in conveyance of water from
G30 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT

the storage facility to the point of utilization. Furthermore, a bias of about 10 percent that results from 

using low-flow frequency curves to compute storage requirements also has been neglected. As the losses and 

the bias both tend to make the computed amount of 

storage smaller than it should be, allowance for these 

must be included in project design. The areal draftstorage relations, therefore, should be used only for 

obtaining preliminary estimates of draft-storage requirements at partial-record sites and for making comparisons between stations. More detailed studies, using 

the data in table 3 if available for the location, should 

be made in connection with design of specific projects.

The curves should not be extrapolated beyond the 

limits to which they are shown.

The procedure used to estimate the draft-storage requirements is described by Speer, Golden, Patterson, 

and others (1964, p. 135-136).

The storage required for a specified draft with a 

chance of its being insufficient on an average of once in 

10 or once in 20 years can be estimated by using figures 7 and 8 and the median annual 7-day low flow 

(Y-day 2-year low flow) for the stream at the point of 

utilization. By using the median annual Y-day low 

flow as abscissa and the storage to be provided as a 

parameter, the diagrams in figures 7A and 8A give the 

specified draft. If the required draft is known, the 

amount of storage required can be estimated from the 

diagrams in figures Y# and 8B.

Illustrative problem, 1. Let it be assumed that a proposal is made to build a manufacturing plant on Castor 

Creek at Castor, La., which will require a minimum flow 

of 6.0 cfs for operation; for economic reasons, the flow 

should not drop below this discharge more often than 

once in 20 years on a long-term average. How much 

storage will be required to maintain this flow for this 

frequency ?

1. From table 2, for Castor Creek at Castor, La. 

(Y-3527), obtain the median annual Y-day low flow 

(Y-day 2-year low flow), which is 0.16 cf s per sq 

mi, and the drainage area, which is 2Y.9 sq mi.

2. Divide 6.0 cfs by 2Y.9 sq mi to obtain a required draft 

of 0.215 cfs per sq mi.

3. Use figure 8B. The abscissa being 0.16 cfs per sq mi 

and the ordinate being 0.215 cfs per sq mi, the 

estimated storage required is 15 acre-ft per sq mi 

or 418 acre-ft. This amount plus 10 percent for 

bias and plus an additional amount for reservoir 

and conveyance losses would be required to provide 

the desired draft and would be insufficient at average intervals of 20 years. 

If it is desired to estimate the maximum draft that

may be made from a specified amount of available storage, the available storage must first be adjusted by estimates of reservoir and conveyance losses, and then the 

drafts that may be expected at the point of utilization 

can be determined.

Illustrative problem 2. Let it be assumed that demands for water are such that they greatly exceed the 

natural flow of Castor Creek at Castor, La., and let it 

be assumed also that upstream from Castor a total storage of Y86 acre-ft could be developed or made available 

for supplementing low flows. What draft at Castor 

can be maintained by this storage if a deficiency once 

in 10 years can be tolerated?

1. From table 2, for Castor Creek at Castor, La. 

(Y-352Y), obtain the drainage area, which is 27.9 

sq mi, and the median annual Y-day low flow (7- 

day 2-year low flow), which is 0.16 cfs per sq mi.

2. Estimate the annual reservoir and conveyance losses 

and deduct these amounts from the total storage. 

For this problem, the total of reservoir and conveyance losses during a dry year and 10 percent 

bias are estimated as 200 acre-ft. The net storage 

available for use at Castor is Y86 acre-ft minus 200 

acre-ft, or 586 acre-ft.

3. Divide the net storage by the drainage area to obtain 

the net acre-feet per square mile available at 

Castor :

586 n. .. =21 acre-ft per sq mi

,

4. Use figure 7 A. The abscissa being 21 acre-ft per sq 

mi, and the parameter being 0.16 cfs per sq mi, 

interpolate between median annual 7-day low-flow 

curves of 0.1 and 0.2 cfs per sq mi, and read as 

ordinate the draft of 0.24 cfs per sq mi. For 27.9 

square miles, this would give 6.7 cfs as the allowable draft that would deplete the storage once in 

10 years on a long-term average. As soon as the 

storage was depleted, the available flow would drop 

to the natural inflow, which for this stream is 

0.12 cfs per sq mi or 3.3 cfs at a 10-year recurrence 

interval, unless the allowable draft were curtailed 

to less than 6.7 cfs as the drought developed and 

as the amount of water in storage became dangerously low. 

Storage and draft data in figure 7 and 8 may be converted to other units by using the following conversion

equivalents :

1 acre- ft= 0.326 million gal= 0.504 cfs-day

1 cf s=1.983 acre-ft per day =0.646 million gal per

day

1 million gal per sq mi =1:548 cfs-days per sq mi= 

3.070 acre-ft per sq mi
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G31

QUALITY OF THE WATER

By H. G. JEFFERT

During periods of low flow, the chemical quality 

of water in streams sampled in the study area is controlled by the composition of the geologic units in the 

drainage basins unless altered by the addition of oilfield wastes. Because of these influences, surface 

waters in the area are extremely variable in the 

character and amounts of dissolved solids. In streams 

where the composition of the geologic units is the 

principal controlling factor on water quality, the 

character and amount of dissolved solids depend primarily on the solubility of the aquifer materials and 

the length of time the water is in contact with these 

materials. In these streams the dissolved-solids content usually is low, and the chemical characteristics of 

the water from each stream are fairly uniform. The 

dissolved-solids content of water in streams that receive 

oil-field wastes is variable, depending upon the relative 

rates of streamflow and the release of wastes.

The dissolved-solids content of water in the streams 

sampled (table 5) ranges from 12 to 12,900 ppm (parts 

per million), hardness from 6 to 1,010 ppm, iron from 

0.00 to 1.2 ppm, fluoride from 0.0 to 2.0 ppm, nitrate 

from 0.0 to 4.0 ppm, and silica from 0.0 to 34 ppm. The 

higher concentrations of dissolved solids and hardness 

are from streams that contain oil-field wastes. Water 

that shows the higher concentrations of iron is also 

highly colored. The maximum concentration of 

fluoride is much higher than would normally be expected, and the source of the fluoride is not known. 

The source and significance of dissolved mineral constituents and properties of water are shown in table 6.

The suitability of water for most uses depends on the 

chemical, biological, and physical characteristics of the 

water. For most industrial and municipal uses, water 

requires some treatment, the degree and type of which 

depend on the quality and intended use of the water. 

In many of the unpolluted streams in this area, the 

water would be suitable for some uses, such as cooling, 

with little or no treatment. However, for municipal and 

most industrial uses, the water would require, as a minimum treatment, pH adjustment for corrosion control, 

and for some water, color and iron removal. Much of 

the water also would require silica removal if it was 

to be used in high-pressure boilers. Because of the present and potential variations in the chemical quality of 

water in streams receiving oil-field wastes, these streams 

generally are not suitable as sources of municipal or industrial water supplies.

The chemical characteristics of water in the streams 

sampled are shown graphically on plate 2. The single

diagram or pattern represents the average of two analyses (table 5) of the water at each site sampled, except 

for Two Prairie Bayou at Carlisle, Ark. (7-2642), Big 

Cypress Creek at Turner, Ark. (7-0779.7), and Black 

Bayou at Benton, La. (7-3498.4), where only one analysis is available at each site. Double patterns are shown 

for Wattensaw Bayou near Hazen, Ark. (7-0769.5), 

and Kelly Creek near Marietta, Tex. (7-3460.2), where 

the water has a more variable composition.

The geologic units contributing water to Ozan Creek 

near McCaskill, Ark. (7-3612), are the Tokio Formation of Cretaceous age and the alluvium of Quaternary 

age. The water is a calcium bicarbonate type (pi. 2); 

this composition indicates that the principal soluble constituent in the aquifer materials is calcium carbonate. 

The variation in dissolved solids of the two analyses, 56 

and 91 ppm (table 5), probably is due to the relative 

amounts of water contributed from each formation. 

Water from Quaternary deposits generally has a higher 

calcium bicarbonate content than water from the outcrop of the Tokio Formation. Thus, the increase in calcium bicarbonate with the decrease in discharge (from 

0.27 to 0,14 cfs) is indicative of a larger percentage of 

the flow coming from the Quaternary deposits. The 

water in Ozan Creek near McCaskill, Ark., is similar 

in chemical characteristics to water in the Little Missouri Kiver near Boughton, Ark. (U.S. Geol. Survey, 

1959b, p. 227-229), and its quality is representative of 

the quality of water in other streams draining areas of 

similar geology.

Walnut Bayou near Foreman, Ark. (7-3369), drains 

the Ozan Formation and alluvium. The water in this 

stream generally is high in dissolved solids and the 

large amounts of sulf ate and chloride indicate that most 

of the dissolved solids in the water are from the Ozan 

Formation.

Low-flow water in the streams that drain Eocene formations, or various combinations of Eocene and Quaternary formations, is variable in dissolved-solids content 

and in chemical characteristics. Water in these streams 

is slightly acid, and where the activities of man have not 

affected the water quality, the water is generally soft 

(0-60 ppm hardness) but has a dissolved-solids content 

of as much as 100 ppm. In many of the streams a 

large part of the variation in dissolved solids is caused 

by the variation in the silica content. Such water does 

not seem to have any chemical characteristic peculiar 

to one formation or a combination of formations. For 

instance, Francois Creek near Poyen, Ark. (7-3631), 

and Prewitt Creek near Karnack, Tex. (7-3460.8), both 

drain the Wilcox and the lower part of the Claiborne 

Group, but the patterns of the chemical analyses for
TABUJ 5. Chemical analyses of low-flow surface waters in the study area

O 

oo

Aquifers in drainage basin 

above sampling station

Tokio Formation and alluvium

Ozan Formation and alluvium

Midway Group

Wilcox Group and lower part of Claiborne 

Group

Wilcox Formation, Carrizo Sand, and 

Reklaw Member of Mount Selman 

Formation

Wilcox Group, Carrizo Sand, and 

Sparta Sand

Wilcox Group and terrace deposits

Wilcox Formation and alluvium

Date of 

collection

Discharge 

(cfs)

Parts per million

Silica 

(SIOi)

Iron

(Fe)

Calcium 

(Ca)

Magnesium 

(Mg)

Sodium 

(Na)

Potassium 

(K)

Bicarbonate 

(HCO3)

Sulfate 

(SO,)

Chloride 

(Cl)

Fluoride 

(F)

Nitrate 

(NOs)

Dissolved 

solids 

(calculated 

from determined 

constituents)

Hardness 

as CaCOs

Calcium, 

magnesium

Noncarbonate

Specific 

conductance (micromhos at 

25°C)

PH Color

7-3612. Ozan Creek near McCaskill, Ark. (drainage area, 148 sq mi)

9- 8-60 

8-15-62 0.27 

.14

0.7 

5.5

0.00 

.01

17 

28

0.8 

1.7

2.0 

2.0

1.6 

1.8

51 

84

6.0 

5.4

3.0 

5.0

0.0 

.2

0.1 

.5

56 

91

46

77

4 

8

101 

165

6.8 

6.4

6 

10

7-3369. Walnut Bayou near Foreman, Ark. (drainage area, 83.6 sq mi)

9-23-60 

8-16-62 0.21 

.10

6.5 

9.8

0.00 

.00

124 

91

30 

19

145 

147

5.2 

3.6

336 

273

167 

117

210 

205

0.5 

.1

0.6

.2

855 

727

433 

305

158 

82

1,480 

1,260

6.9 

8.1

5 

4

7-3369.5. Barkman Creek near Leary, Tex. (drainage area, 31.5 sq mi)

5-23-61 

9-18-62 2.34 

.90

5.7 

12

0.00 

.03

6.4 

7.2

2.4 

1.8

11 

13

2.1 

2.6

35 

36

3.8 

6.8

9.0 

10

0.3 

2.0

1.0

.2

59

74

26 

25

0 

0

108 

129

6.2 

6.3

45 

30

7-3631. Francois Creek near Poyen, Ark. (drainage area, 84.1 sq mi)

9-20-60 

6-27-61 0.05 

5.24

1.6 

5.9

6.4 

6.4

1.3 

1.9

9.0 

9.4

2.0 

1.1

16 

10

23 

36

3.0 

1.0

0.1 

.0

0.3 

.6

54 

67

22 

24

8 

16

109 

107

6.3 

6.4

7 

5

7-3460.8. Prewitt Creek near Karnack, Tex. (drainage area, 29.5 sq mi)

5-23-61 

9-19-62 3.18 

.49

12 

18

0.00 

.04

2.7 

3.0

1.5 

1.9

3.7 

3.3

0.7

1.2

12 

13

5.2 

4.8

4.0 

5.5

0.2 

.1

1.3 

.0

37 

44

12 

15

2 

5

47 

48

6.2 

6.2

20 

15

7-3617. Caney Creek near Bluff City, Ark. (drainage area, 167 sq mi)

9- 8-60 

8-15-62 0.66 

.30

0.0 

2.9

0.00 

.00

58 

69

16 

19

580 

561

9.5 

12

30

2

18 

14

1,040 

1,050

0.9 

.3

0.7 

.4

1,740 

1,730

210 

250

186 

249

3,400 

3,350

6.5 

5.4

7 

4

7-3482. Paw Paw Bayou near Greenwood, La. (drainage area, 78 sq mi)

5-16-61 

3- 7-63 2.56 

10.6

6.7 

4.7 0.11

28 

31

13

17

100 

113

3.5 

5.3

86 

40

37 

64

165 

205

0.2 

.0

1.0 

1.0

396 

461

124 

148

53 

115

741 

890

7.0 

6.6

15 

50

7-3516.7. Rambin Bayou near Frierson, La. (drainage area, 59.6 sq mi)

5-16-61 

3- 8-63 10.5 

4.79

7.7 

4.9 6.04

25 

22

13

12

61 

37

3.6

4.8

100 

66

70 

61

70 

51

0.1 

.0

1.2 

1.2

301

226

116 

105

34 

50

511 

394

7.2 

6.9

10 

40

7-3441. Caney Creek near Red water, Tex. (drainage area, 18 sq mi)

5-23-61 

9-18-62 3.90 

.57

17 

22

0.00 

.03

5.2 

9.0

3.0 

2.9

13. 

9.4

1.2 

1.9

40 

45

4.0 

5.4

12 

10

0.2 

.2

0.9 

.0

76 

83

26 

34

0 

0

113 

114

6.5 

6.3

40 

15
7-3601. L'Eau Frais Creek at Joan, Ark. (drainage area, 79.4 sq mi)

Lower part of Claiborne Group

Carrizo Sand and Reklaw and Queen City 

Sand Members of Mount Selman Formation

Queen City Sand Member of Mount Selman 

Formation

Queen City Sand and Weches Greensand 

Members of Mount Selman Formation and 

Sparta Sand

Queen City Sand and Weches Greensand 

Members of Mount Selman Formation, 

Sparta Sand, and terrace deposits

Sparta Sand

Sparta Sand and terrace deposits

Sparta Sand and alluvium

9-6-60 

8-13-62 2.73 

3.94

0.5 

6.3

0.00 

.04

1.7 

1.9

0.5 

.6

1.3 

1.7

0.8 

1.0

7 

6

1.2

2.8

2.0 

3.0

0.3 

.2

0.6 

.6

12 

21

6

7

0 

2

23 

26

6.3 

6.4

15 

5

7-3460.2. Kelly Creek near Marietta, Tex. (drainage area, 50.5 sq mi)

5-23-61 

9-18-62 6.21 

.39

14 

29

0.00 

.01

2.9 

6.2

1.6 

2.5

3.7 

4.9

1.3

2.8

12 

2

5.6

28

3.5 

6.0

0.2 

.1

2.6 

.0

41 

81

14 

26

4 

24

49 

93

6.1 

5.4

0 

15 ^ 

5 ^

>Ti

F 7-3460.4. Hughes Creek near Avinger, Tex. (drainage area, 48.6 sq mi) O 

<1

5-23-61 

9-18-62 9.86 

7.99

10 

22

0.00 

.02

2.5 

2.5

1.5 

2.0

3.7 

5.3

1.2 

2.3

10 

15

5.0 

6.4

5.0

7.2

0.0 

.1

1.5 

.0

35 

55

12 

14

4 

2

47 

62

5.8 

5.8

-s 

7 M 

15 §

CQ 

7-3460.6. Moccasin Creek near Harleton, Tex. (drainage area, 30.5 sq mi) O 

d

5-23-61 

9-19-62 1.38 

.56

19 

34

0.00 

.02

3.8 

4.5

1.8 

2.2

8.8 

7.3

1.4 

3.7

10 

10

7.2 

17

14 

10

0.1 

.2

1.3 

. .2

62 

84

17 

20

9 

12

87 

95

5.8 

5.7

12 3 

15 M

7-3463.2. Black Bayou near Atlanta, Tex. (drainage area, 52.1 sq mi) 

h>.

5-23-61 

9-18-62 8.06 

4.90

10 

19

0.00 

.05

3.0 

4.2

1.9 

1.8

19 

31

1.7 

2.9

36 

53

3.8 

3.4

15

27

0.3 

.2

2.9 

40

76 

120

16 

18

0 

0

121 

189

6.7 

6.2

30 W 

25 £ 

5

02 7-3464. Black Bayou near Rodessa, La. (drainage area, 113 sq mi) |> 

in

11-18-60 5-15-61 3.57 

2.08

4.1

8.6

0.96 3.5 

4.0

0.8 

1.2

6.1 

5.4

2.0 

1.0

12 

20

6.0 

2.0

7.8 

7.0

0.4 

.0

1.3

.7

39 

40

12 

15

2 

0

60 

59

6.1 

6.5

80 H, 

40 §

M

7-3520. Saline Bayou near Lucky, La. (drainage area, 154 sq mi) !"§

11-17-60 8-15-62 24.7 

12.2

3.8 

14

0.22 

.01

3.6 

3.5

0.4 

1.6

14 

22

1.1

.8

10

7

0.0 

.2

23 

41

0.5 

.0

1.0 

.0

52 

86

10 

15

2 

10

101 

159

6.0 

5.5

H 

45 W 

5 ^-\

7-3708.2. Dugdemona River near Quitman, La. (drainage area, 117 sq mi) O 

d

11-13-60 8-15-62 3.50

.284

5.0 

20

1.2 

.05

3.2

7.2

0.7 

3.4

3.2

5.7

2.1 

2.6

14 

41

4.2 

3.0

2.8 

7.1

0.2 

.1

1.4 

.2

31 

69

11 

32

0 

0

40 

92

6.3 

6.0

150 | 

25 g

7-3491. Brushy Creek near Sibley, La. (drainage area, 43.6 sq mi) 

»

11-11-60 5-23-61 5.91 

9.46

5.9 

9.8

0.06 41 

3.8

1.4 

1.6

11 

8.9

4.0 

1.2

9 

13

3.4 

1.6

22 

18

0.3 

.0

0.9 

.9

58 

52

16 

16

8 

6

96 

84

6.3 

6.3

25 S 

15 i-q 

M

7-3619. Bayou Freeo near Eagle Mills, Ark. (drainage area, 94.8 sq mi) >£ 

rn

9- 6-60 

8-13-62 1.68 

.43

5.0 

14

0.00 

.22

4.9 

4.5

0.7 

2.4

3.7 

5.3

1.8 

2.4

18 

30

3.2 

4.8

3.8 

3.2

0.0 

.3

0.3 

.6

32 

52

15 

21

0 

0

51 

75

6.7 

7.1 30 g

7-3618.5. Tulip Creek near Pine Grove, Ark. (drainage area, 152 sq mi) 1-3

9- 6-60 

8-13-62 2.64 

4.17

5.7 

7.3

0.06 

.02

3.2 

3.2

0.5 

1 0

1.4 

2.2

1.1 

1.4

12 

14

2.6 

3.2

1.8 

2.2

0.1 

.3

0.8 

.3

23

28

10 

12

0 

0

31 

37

6.4 

6.6

20 £ 

10 GO

O
TABLE 5. Chemical analyses of low-flow surface waters in the study area Continued

o

Aquifers in drainage basin 

above sampling station

Cook Mountain Formation

Cook Mountain and Cockfleld Formations

Cockfleld Formation

Cockfleld Formation and alluvium

Date of collection

Discharge 

(cfs)

Parts per million

Silica 

(SIOi)

Iron 

(Fe)

Calcium 

(Ca)

Magnesium 

(Mg)

Sodium 

(Na)

Potassium 

(K)

Bicarbonate 

(HCOa)

Sulfate 

(S0<)

Chloride 

(Cl)

Fluoride 

(F)

Nitrate 

(NOs)

Dissolved 

solids (calculated 

from determined 

constituents)

Hardness 

as CaCOs

Calcium, 

magnesium

Noncarbonate

Specific 

conductance 

(micromhos at 

25°C)

pH Color

7-3651. Cypress Creek near TTnionville, La. (drainage area, 63.3 sq mi)

11-18-60 8-17-62 0.203 

.53

1.4 

11

0.58 

.03

5.1 

5.2

1.9 

2.6

27 

43

4.8 

3.8

50 

71

22 

15

14 

32

0.3 

.4

1.7 

.2

104 

148

20 

24

0 

0

177 

253

6.8 

6.2

65 

10

7-3649. Big Creek near Vienna, La. (drainage area, 68.9 sq mi)

10-18-60 4-19-63 0.193 

10.7

1.8 

5.4

1.2 

.14

3.6 

4.9

0.9 

1.8

2.5 

3.3

2.2 

1.6

11 

16

7.2 

8.0

2.8 

5.8

0.1 

.0

1.7 

.6

29 

39

12 

20

4 

6

43 

62

6.7 

6.8

250 

45

7-3648. Bayou D'Arbonue at Homer, La. (drainage area, 30 sq mi)

10-13-60 9-21-62 1.57 

1.49

4.2 

19

0.24 

.06

2.2 

1.5

1.1 

1.4

3.8 

3.0

2.2 

1.7

11

8

4.8 

2.4

4.8 

6.1

0.1 

.1

0.9 

.5

30 

40

10 

10

0 

3

46 

38

6.5 

5.4

60 

25

7-3653. Middle Fork Bayou D'Arbonne near Colquitt, La. (drainage area, 43.9 sq mi)

10-13-60 9-21-62 0.866 

3.71

6.4 

18

0.00 

.10

26 

15

6.5 

4.1

58 

46

5.0 

2.8

14 

10

9.2 

6.0

142 

103

0.2 

.2

1.3 

.0

262 

200

92 

54

80 

46

527 

369

6.0 

5.7

10 

5

7-3647.5. Bayou de Loutre at De Loutre, La. (drainage area, 302 sq mi)

11-4-60 

8-14-62 34.1 

10.3

1.4 

7.3

0.00 

.01

307 

249

42 

34

939

866

33

16

68 

47

55 

60

2,050 

1,830

0.9 

1.0

0.3 

1.5

3,460 

3,090

938 

762

883 

723

6,330 

5,660

6.6 

6.5

22 

15

7-3664. Bayou Choudrant at Tremont, La. (drainage area, 87.5 sq mi)

10-14-60 8-14-62 1.69 

4.64

6.8 

15

0.15 

.04

2.4 

2.0

0.6 

1.3

2.7 

2.6

1.5 

1.3

11 

11

1.0 

1.2

3.5

4.8

0.2 

.0

0.9 

1.0

25 

34

14 

10

4 

1

35 

34

6.3 

5.9

35 

15

7-3658.5. Little Corney Bayou near Summerfleld, La. (drainage area, 54 sqmi)

11-17-60 8-15-62 6.18 

.17

7.3

16

0.04 

.09

12 

13

2.3 

2.6

22 

12

3.2 

2.4

10 

34

5.2 

2.6

54 

29

0.2 

.1

0.8 

.0

112 

95

40 

43

32 

15

213 

164

6.0 

6.0

25 

10

7-3673. North Cheniere Creek at Cheniere, La. (drainage area, 38 sq mi)

10-11-60 8-14-62 4.51 

2.32

7.1 

15

0.13 

.01

5.6 

2.5

0.1 

1.4

8.3 

3.0

1.5 

1.5

9 

11

4.4 

.2

16 

7.0

0.2 

.1

0.8 

1.0

48 

37

14 

12

7 

3

112 

41

6.5 

5.5

40 

10

I

00 

O 

ej

GO

I

00

H
7-2642. Two Prairie Bayou at Carlisle, Ark. (drainage area, 149 sq mi)

Terrace deposits

Terrace deposits and alluvium

Alluvium

7-11-61 13.6 8.3 19 7.1 18 3.2 108 11 14 0.3 1.4 135 76 0 229 7.3 10

7-3498.4. Black Bayou at Benton, La. (drainage area, 17.2 sq ml)

5-23-61 0 2.4 19 8.8 29 3.5 96 12 40 0.2 1.4 163 84 5 295 7.1

f 

20 O

7-3492. Clarke Bayou near Haughton, La. (drainage area, 35.1 sq mi) w

5-23-61 

8-17-62 0.52 

.16

0.9

8.1 0.02

220 

76

113

47

4,620 

2,440

79 

20

300 

204

141 

4.9

7,540 

3,860

0.4 12,900 

6,560

1,010 

383

768 

216

21,600 

11,200

7.5 

6.8

O

10 3

20 ^

H

i4 

7-0779.7. Big Cypress Creek at Turner, Ark. (drainage area, 125 sq ml) 

rn

10-26-60 5.0 0.00 15 6.8 14 5.1 80 11 18 0.3 1.2 115 66 0 210 6.7

O

6 d hi M-i 

7-0769.5. Wattensaw Bayou near Hazen, Ark. (drainage area, 195 sq mi) (S rl

9-12-61 

4-18-63 17.1 

18.9

10 

2.4 0.36

20 

5.9

7.8 

2.6

18 

4.8

3.1 

3.9

124

28

4.2 

3.4

13 

5.5

0.3 

.0

0.9 

2.1

138 

45

82 

25

0 

2

227 

72

7.2 

7.0

10 

90 >

W 

7-3642.5. Chemin-a-Haut Creek near Berlin, Ark. (drainage area, 216 sq ml) b». £ 

9-20-60 

8-13-62 4.11 

1.61

4.5 

4.9

0.00 

.02

30

25

7.0

8.6

22 

20

3.6 

3.8

146 

139

2.6 

4.2

21 

20

0.2 

.2

0.6 

.6

164 

156

104 

98

0 

0

278 

278

7.3

7.8

53

20 > 

10 J»

7-3643. Chemin-a-Haut Bayou (Creek) near Beekman, La. (drainage area, 271 sq ml) g

11-14-60 8-14-62 20.3 

3.82

0.9 

11

0.00 

.12

19 

24

5.8 

7.6

17 

23

4.3 

3.4

100 

132

1.4

2.8

20 

23

0.4 

.2

1.0 

.2

119 

160

72 

91

0 

0

219

289

7.1 

6.4

VJ

17 £j 

5 §

kH

7-3685.2. Big Creek at Holly Ridge, La. (drainage area, 71 sq ml) ^

10-11-60 8-16-62 0.23 

2.16

0.9 

6.5

0.15 

.20

5.4

4.8

1.3

1.8

2.0 

2.1

4.3

4.1

23 

24

3.4

4.2

2.5

2.8

0.2 

.2

2.0

.8

33 

40

19 

19

0 

0

55 

65

6.7 

6.1

r

100 2 

80 2 

QD

> 

0

O
G36 WATER RESOURCES OF THE MISSISSIPPI EMBAYMENT 

TABLE 6. Source and significance of dissolved mineral constituents and properties of water

Constituent or property Source or cause Significance

Silica (S102).

Iron (Fe).

Manganese (Mn).

Calcium (Ca) and magnesium (Mg).

Sodium (Na) and potassium (K).

Bicarbonate (HCOs) and 

carbonate (COs).

Sulfate (S04).

Chloride (Cl).

Fluoride (F).

Dissolved from practically all rocks 

and soils, commonly less than 30 

ppm. High concentrations, as 

much as 100 ppm, generally occur 

in highly alkaline waters.

Dissolved from practically all rocks 

and soils. May also be derived 

from iron pipes, pumps, and other 

equipment. More than 1 or 2 ppm 

of soluble iron in surface waters 

generally indicates acid wastes from 

mine drainage or other sources.

Dissolved from some rocks and soils. 

Not so common as iron. Large 

quantities often associated with 

high iron content and acid waters.

Dissolved from practically all rocks 

and soils, but especially from limestone, dolomite, and gypsum. Calcium and magnesium are found in 

large quantities in some brines. 

Magnesium is present in large quantities in sea water.

Dissolved from practically all rocks 

and soils. Found also in ancient 

brines, sea water, industrial brines, 

and sewage.

Action of carbon dioxide in water on 

carbonate rocks such as limestone 

and dolomite.

Dissolved from rocks and soils containing gypsum, iron sulfides, and 

other sulfur compounds. Commonly present in mine waters and 

some industrial wastes.

Dissolved from rocks and soils. Present in sewage and found in large 

amounts in ancient brines, sea 

water, and industrial wastes.

Dissolved in small to minute quantities from most rocks and soils. 

Added to many waters by fluoridation of municipal supplies.

Forms hard scale in pipes and boilers. Carried over in 

steam of high-pressure boilers to form deposits on blades 

of turbines. Inhibits deterioration of zeolite-type water 

softeners.

More than about 0.3 ppm stains laundry and utensils reddish 

brown. Objectionable for food processing, textile processing, beverages, ice manufacture, brewing, and other 

processes. TJSPHS (1962) 1 drinking-water standards state 

that iron should not exceed 0.3 ppm. Larger quantities 

cause unpleasant taste and favor growth or iron bacteria.

Same objectionable features as iron. Causes dark brown 

or black stain. TJSPHS (1962) drinking-water standards 

state that manganese should not exceed 0.05 ppm.

Cause most of the hardness and scale-forming properties of 

water; soap consuming (see Hardness). Waters low in 

calcium and magnesium desired in electroplating, tanning, 

and dyeing and in textile manufacturing.

Large amounts, in combination with chloride, give a salty 

taste. Moderate quantities have little effect on the usefulness of water for most purposes. Sodium salts may 

cause foaming in steam boilers, and a high sodium content 

may limit the use of water for irrigation.

Bicarbonate and carbonate produce alkalinity. Bicarbonates of calcium and magnesium decompose in steam 

boilers and hot-water facilities to form scale and release 

corrosive carbon dioxide gas. In combination with 

calcium and magnesium they cause carbonate hardness.

Sulfate in water containing calcium forms hard scale in 

steam boilers. In large amounts, sulfate in combination 

with other ions gives a bitter taste to water. Some 

calcium sulfate is considered beneficial in the brewing 

process. USPHS (1962) drinking-water standards recommend that the sulfate content should not exceed 250 ppm.

In large amounts in combination with sodium gives salty 

taste to water. In large quantities increases the corrosiveness of water. TJSPHS (1962) drinking-water standards recommend that the chloride content not exceed 250 

ppm.

Fluoride in drinking water reduces the incidence of tooth 

decay when the water is consumed during the period of 

enamel calcification. However, it may cause mottling 

of the teeth depending on the concentration of fluoride, 

the age of the child, the amount of water consumed, and 

the susceptibility of the individual. The maximum concentration of fluoride recommended by the TJSPHS (1962) 

varies with the annual average of maximum daily air 

temperatures and ranges downward from 1.7 ppm for an 

average maximum daily temperature of 50.0°F to 0.8 

ppm for an average maximum daily temperature of 

90.5°F. Optimum concentrations for these ranges are 

from 1.2 to 0.7 ppm.
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS 

TABLE 6. Source and significance of dissolved mineral constituents and properties of water Continued

G37

Constituent or property Source or cause Significance

Nitrate (NO3).

Dissolved solidsHardness as CaCOsSpecific conductance (micromhos at 25°C).

Hydrogen-ion concentration (pH).

Color.

TemperatureSuspended sedimentDecaying organic matter, legume 

plants, sewage, nitrate fertilizers, 

and nitrates in soils.

Chiefly mineral constituents dissolved 

from rocks and soils.

In most waters, nearly all the hardness is due to calcium and magnesium. All the metallic cations 

other than the alkali metals also 

cause hardness.

Mineral content of the waterAcids, acid-generating salts, and free 

carbon dioxide lower the pH. Carbonates, bicarbonates, hydroxides, 

phosphates, silicates, and borates 

raise the pH.

Yellow-to-brown color of some water 

usually is caused by organic matter 

extracted from leaves, roots, and 

other organic substances. Color in 

water also results from industrial 

wastes and sewage.

Climatic conditions, use of water as a 

cooling agent, industrial pollution.

Erosion of land and stream channels. 

Quantity and particle-size gradation 

affected by many factors such as 

form and intensity of precipitation, 

rate of runoff, stream channel and 

flow characteristics, vegetal cover, 

topography, type and characteristics 

of soils in drainage basin, agricultural practices, and some industrial and mining activities. Largest 

concentrations and loads occur during periods of storm runoff.

Concentration much greater than the local average may 

suggest pollution. USPHS (1962) drinking-water standards suggest a limit of 45 ppm. Waters of high nitrate 

content have been reported to be the cause of methemoglobinemia (an often fatal disease in infants) and therefore 

should not be used in infant feeding. Nitrate has been 

shown to be helpful in reducing the intercrystalline cracking of boiler steel. It encourages the growth of algae and 

other organisms which may cause odor problems in water 

supplies.

USPHS (1962) drinking-water standards recommend that 

the dissolved solids should not exceed 500 ppm. However, 

1,000 ppm is permitted under certain circumstances. 

Waters containing more than 1,000 ppm of dissolved 

solids are unsuitable for many purposes.

Consumes soap before a lather will form. Deposits soap 

curd on bathtubs. Hard water forms scale in boilers, 

water heaters, and pipes. Hardness equivalent to the 

bicarbonate and carbonate is called carbonate hardness. 

Any hardness in excess of this is called noncarbonate 

hardness. Waters of hardness up to 60 ppm are considered soft; 61-120 ppm, moderately hard; 121-180 ppm, 

hard; more than 180 ppm, very hard.

Indicates degree of mineralization. Specific conductance 

is a measure of the capacity of the water to conduct an 

electric current. It varies with the concentration and 

degree of ionization of the constituents, and with 

temperature.

A pH of 7.0 indicates neutrality of a solution. Values 

higher than 7.0 denote increasing alkalinity; values lower 

than 7.0 denote increasing acidity. pH is a measure of 

the activity of hydrogen ions. Corrosiveness of water 

generally increases with decreasing pH. However, excessively alkaline water may also attack metals.

Water for domestic and some industrial uses should be free 

from preceptible color. Color in water is objectionable 

in food and beverage processing and many manufacturing 

processes.

Affects usefulness of water for many purposes. Most users 

desire water of uniformly low temperature. Seasonal 

fluctuations in temperatures of surface waters are comparatively large depending on the volume of water.

Sediment must generally be removed by flocculation and 

filtration before water is used by industry or municipalities. 

Sediment deposits reduce the storage capacity of reservoirs 

and lakes and clog navigable stream channels and harbors. 

Particle-size distribution is a factor controlling the density 

of deposited sediment and is considered in the design of 

filtration plants. Sediment data are of value in designing 

river-development projects, in the study of biological 

conditions and fish propagation, and in programs of soil 

conservation and watershed management.

* "Public Health Service Drinking Water Standards," revised 1962, apply to drinking water and water-supply systems used by carriers and others subject to Federal quarantine regulations.
G38 WATER RESOURCES ()F THE MISSISSIPPI EMBAYMENT

these two streams (pi. 2) show no resemblance to each 

other. Calcium, sodium, and sulfate are the predominant constituents in water from Francois Creek, 

whereas no constituent predominates in water from Prewitt Creek. One of the patterns shown for Kelly Creek 

near Marietta, Tex. (7-3460.2), resembles the pattern 

shown for Francois Creek near Poyen, Ark., in that 

sulfate is the predominant anion. Kelly Creek drains 

the Carrizo Sand 'and the Reldaw and the Queen City 

Sand Members of the Mount Selman Formation.

Variability in the type of water in streams receiving 

their base flow from the same formation is also shown 

in the patterns for Saline Bayou near Lucky, La. 

(7^3520), Brushy Creek near Sibley, La. (7-3491), 

and Dugdemona River near Quitman, La. (7-3708.2). 

These three streams drain the Sparta Sand, but the 

pattern for Dugdemona River shows the water to be 

more like water from Big Creek at Holly Ridge, La. 

(7-3685.2), which drains the alluvium.

Except where oil-field wastes are present, water in 

streams draining alluvium and terrace deposits generally is a calcium-magnesium bicarbonate type. The 

dissolved-solids content of waiter in these streams ranges 

from 33 to 164 ppm. The dissolved-solids content of 

water in streams draining terrace deposits or a combination of terrace deposits and alluvium generally is 

higher than that of water in streams draining only the 

alluvium. Except for one sample from Wattensaw 

Bayou near Hazen, Ark. (7-0769.5), the dissolvedsolids content of water from streams draining the terrace deposits and alluvium ranges from 115 to 164 ppm, 

whereas the maximum dissolved-solids content of water 

from the stream that drains only alluvium is 40 ppm. 

One sample from Wattensaw Bayou near Hazen, Ark., 

has a dissolved-solids content of 45 ppm. This value 

does not seem representative of the dissolved-solids content of water in this stream during low flow, and it is 

likely that the dissolved-solids content on this day 

(Apr. 18,1963) was affected by rain that fell a few days 

prior to the sampling date.

The chemical quality of water in Caney Creek near 

Bluff City, Ark. (7-3617), Clarke Bayou near Haughton, La. (7-3492), Paw Paw Bayou near Greenwood, 

La. (7-3482), Rambin Bayou near Frierson, La. 

(7-3516.7), Bayou de Loutre at De Loutre, La. 

(7-3647.5), and Middle Fork Bayou D'Arbonne near 

Colquitt, La. (7-3653), is affected by the addition of oilfield wastes. The dissolved-solids content of water in 

these streams ranges from 226 to 12,900 ppm. Sodium 

and chloride are the principal constituents, but when 

the dissolved solids are low, the chemical characteristics 

are variable. Because of numerous active oil fields in

southern Arkansas and northern Louisiana, many 

streams other than those listed may contain wastes, but 

it is beyond the scope of this study to determine the degree of contamination of streams in the area.

CONCLUSIONS AND RECOMMENDATIONS

1. Knowledge of the low-flow characteristics of 

streams in the Mississippi embayment in southern 

Arkansas, northern Louisiana, and northeastern Texas 

is useful in the solving of water problems and for the 

economic development of surface-water supplies in the 

area. The need for further development of water resources was 'accentuated by the drought of the 1950's and 

has increased rapidly in recent years. In some areas 

the use of surface water and the creation of numerous 

reservoirs have greatly altered the low-flow characteristics of the streams. As agriculture and industry continue to expand, the affected areas may be expected to 

increase in number and become more widespread. The 

total water resources of the area are sufficient to meet 

the needs for many years in the future, and the anticipated problems of water supply will be those of 

distribution and providing storage to meet the demands 

during periods of low flow. The data presented in this 

chapter provide a suitable basis for planned development of the water resources and for water management, 

but further investigations may be needed for detailed 

design. Estimates of future events based on the data 

in this report will be reasonably reliable provided there 

are no appreciable changes in the hydrologic regime.

2. Comparison of the low-flow characteristics of the 

streams is made on the basis of unit runoff per square 

mile. Because of the wide variation in the yield of the 

streams, and even of the same stream, it is not possible 

to generalize that in an area where one stream shows an 

index of a given yield, all streams in the area have the 

same index. Interpolation of low-flow data presented 

in this chapter should not be made to estimate the low 

flow at ungaged sites on the basis of drainage area without the aid of low-flow discharge measurements at the 

sites and without a knowledge of the geology, physiography, mamnade changes, and other factors affecting 

the low flow.

3. The wide variations in the low-flow indices of the 

streams in the area may be largely attributed to the 

depth to which the streams are incised, the relation of 

the water table to the bed of the stream, and the 

porosity and permeability of the aquifers in the immediate area.

4. As indicated by the data in this chapter, the geologic units that contribute appreciable water to the low 

flow of streams in the study area are (in order of
LOW FLOW IN SOUTHERN ARKANSAS, NORTHERN LOUISIANA, NORTHEASTERN TEXAS G39

decreasing volume contributed): Paleozoic rocks, 

sand units in the Claiborne Group, and Quaternary 

alluvium.

Streams that head in the Paleozoic rocks, particularly 

in the Ouachita Mountains, have high low-flow indices. 

The decrease in the low flow of some streams as they enter the broad alluvial valleys in the embayment may in 

part be due to flow entering the unconsolidated materials in the streambed. Studies to determine the magnitude of such underflow may reveal additional flows suitable for utilization.

The terrace deposits west of Crowleys Kidge in the 

northern part of the study area have indices of zero. 

In general, the streams receiving ther base flow from 

the alluvium and terrace deposits have low indices of 

low flow, but the indices are slightly higher for streams 

south of lat 32°30' N. in the southeast corner of the 

study area.

Overdevelopment of ground-water supplies in the 

Grand Prairie region is shifting the emphasis on water 

supply to surface-water sources. The low-flow characteristics of the small streams in the region, however, 

indicate that surface storage will be required if the 

streams are to supply water during droughts.

In most other sections of the embayment, ground 

water has not been overdeveloped and the demands on 

surface supplies are not so pronounced. Surface water 

is utilized where a dependable supply is readily available. In many places, a combination of ground-water 

and surface-water supplies is used.

Streams in Louisiana lying between the Mississippi 

River and Bayou La Fourche have high low-flow indices because these streams are incised into aquifers in 

the alluvium.

Streams in the southwestern part of the study area 

generally have very low indices of low flow. Most of 

these streams are not incised sufficiently deep to be in 

contact with the water-yielding deposits.

5. The median annual 7-day low flow serving as an 

index, areal draft-storage relations for 10- and 20-year 

recurrence intervals provide a convenient means for 

estimating the storage required to maintain a given 

minimum flow. The relations are valid for median 

annual 7-day low flow of as much as 0.40 cfs per sq mi 

and for storage of as much as 90 acre-ft per sq mi. 

Application of these relations is not recommended for 

intermittent streams or for daily-record gaging sites.

6. The chemical quality of water in streams in the 

study area is controlled by the composition of the geologic units in the drainage basins unless altered by the 

addition of oil-field wastes.

In streams where the composition of the geologic units 

is the controlling factor, the dissolved-so'lids content of 

the water usually is low and the chemical characteristics 

of individual streams are fairly uniform. Water in 

streams draining the Tokio Formation and the alluvium 

is low in dissolved solids and is a calcium bicarbonate 

type. Where the activities of man have not affected 

water quality, water in streams draining formations 

of Eocene age generally is low in dissolved solids. Variations in dissolved solids are caused, to a large extent, 

by variations in the silica content. Streams draining 

Eocene formations do not seem to have any characteristics peculiar to one formation or a combination of 

formations. The chemical characteristics of water in 

streams draining deposits of Quaternary age are fairly 

uniform, but as the dissolved-solids content increases, calcium and bicarbonate become the principal 

constitutents.

The addition of oil-field wastes has adversely affected 

the quality of water in many streams that drain areas 

in southern Arkansas and northern Louisiana.

7. Data are needed to define additional causative 

phases of the hydrologic systems and to forecast the 

effect that future changes in the stream systems may 

have upon the low-flow regimen of the streams. These 

phases include the effect of floods upon the water table 

adjacent to the streams, the effect of swamp environment on the yield from or recharge to the aquifers, the 

effect of deepening or widening of stream channels upon 

the regimen of low flow of the streams and upon the 

ground-water table adjacent to the streams, the magnitude of underflow in the alluvial valleys, the interrelations between the ground-water fluctuations and the low 

flow of streams, and the effect of impoundment of water 

in ponds and reservoirs upon the low flow of the streams. 

The results of the study reported in this chapter indicate that increases or decreases in low flow probably 

have resulted from manmade changes. More detailed 

knowledge of the geology is needed to define the aquifers 

or water-bearing geologic units that underlie the drainage basins in much of the area.

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