WATER-RESOURCES APPRAISAL OP THE LAKE TRAVERSE 

INDIAN RESERVATION IN SOUTH DAKOTA

By Stephen J. Lawrence

U.S. GEOLOGICAL SURVEY

Water-Resources Investigations Report 88-4031

Huron, South Dakota 

1989
DEPARTMENT OF THE INTERIOR 

MANUEL LUJAN, JR., Secretary

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director

For additional information 

write to:

District Chief 

U.S. Geological Survey 

Rm. 408, Federal Bldg. 

200 4th St. SW 

Huron, SD 57350

Copies of this report can 

be purchased from:

U.S. Geological Survey 

Books and Open-File Reports 

Federal Center, Bldg. 810 

Box 25425 

Denver, CO 80225-0425
CONTENTS

Page

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

Introduction .............................. 1

Physiography ........................... 2

Climate .............................. 2

Geology .............................. 6

Surface water .............................. 6

Surface-water quantity ....................... 15

Streams ............................ 15

Lakes ............................. 21

Surface-water quality ....................... 21

Streams ............................ 21

Lakes ............................. 27

Ground water .............................. 31

Hydrogeology ............................ 32

Ground-water quality ........................ 35

Needed additional studies ........................ 38

Summary ................................. 40

Selected references ........................... 41
ILLUSTRATIONS

Page

Figure 1. Map showing the location of the Lake Traverse Indian

Reservation in South Dakota ................. 3

2. Map showing physiographic divisions in and near the

Lake Traverse Indian Reservation ............... 4

3. Graphs showing 30-year (1951-80) mean monthly precipitation 

and the 95th-percentile value for selected sites in 

and near the Lake Traverse Indian Reservation ........ 5

4. Map showing bedrock geology in and near the

Lake Traverse Indian Reservation ............... 7

5. Map showing glacial deposits of Pleistocene and Holocene

age in and near the Lake Traverse Indian Reservation ..... 8

6. Geologic section across the northern part of the

Lake Traverse Indian Reservation ............... 9

7. Map showing contributing drainage area of the Big 

Sioux River basin upstream from confluence with 

Mud Creek and location of streamflow-gaging stations 

in the contributing part of the basin in and near 

the Lake Traverse Indian Reservation ............. 11

8. Map showing noncontributing drainage areas of the Big 

Sioux and James River basins and location of selected 

lakes in and near the Lake Traverse Indian Reservation .... 12

9. Map showing drainage area of the Souris-Red-Rainy River 

basin and location of streamflow-gaging stations in 

and near the Lake Traverse Indian Reservation ........ 13

10. Map showing drainage area of the Upper Mississippi

River basin and location of streamflow-gaging stations

in and near the Lake Travervse Indian Reservation ...... 14

11. Graphs showing statistics of mean daily discharge for

the period of record at three streamflow-gaging stations

in and near the Lake Traverse Indian Reservation ....... 16

12. Graphs showing statistics of cumulative runoff for the 

period of record at three streamflow-gaging stations 

in and near the Lake Traverse Indian Reservation ....... 19

13. Graphs showing 7-day, 10-year and 15-day, 10-year minimum 

discharges for the period of record at three streamflowgaging stations in and near the Lake Traverse Indian 

Reservation ......................... 20

14. Graphs showing lake levels and corresponding total

rainfall at Sisseton for water years 1936-76 ......... 23

15. Diagrams of water quality at three stream sites in and

near the Lake Traverse Indian Reservation .......... 24

16. Diagrams of water quality of four lakes in and near

the Lake Traverse Indian Reservation ............. 28

17. Map showing depth below land surface and thickness 

of sand and gravel deposits in the 

Lake Traverse Indian Reservation ............... 33

18. Map showing water-table altitude in surficial sand or

gravel in the Lake Traverse Indian Reservation ........ 34

19. Diagrams of ground-water quality by well depth for

wells in and near the Lake Traverse Indian Reservation .... 36

20. Trilinear plot of water chemistry by well depth for

wells in and near the Lake Traverse Indian Reservation .... 39

xv
TABLES

Table 1. Streamflow-gaging stations operated by the U.S. Geological 

Survey in and near the Lake Traverse Indian Reservation

2. Magnitude and recurrence interval of instantaneous 

peak flow at gaging stations in and near the Lake 

Traverse Indian Reservation ...............

3. Physical characteristics of selected lakes in and near

the Lake Traverse Indian Reservation ...........

4. Summary of water-quality data for the Bois de Sioux

River near White Rock ..................

5. Lakes in and near the Lake Traverse Indian Reservation

grouped by median concentrations of dissolved solids . . .

Page

. 15

18

22

26

30

CONVERSION FACTORS

For readers who may prefer to use metric (International System) units 

rather than inch-pound units, the conversion factors for the inch-pound units 

used in this report are listed below:

Multiply inch-pound unit

acre

acre-foot (acre-ft)

cubic foot per second

(ft 3 /s) 

foot (ft)

foot per mile (ft/mi) 

inch

mile (mi)

mile per hour (mi/h) 

square mile (mi 2 )

By.

0.4047

1,234

0.02832

0.3048

0.1894

25.4

1.609

1.609

2.590

To obtain metric unit

hectare

cubic meter

cubic meter per second

meter

meter per kilometer

millimeter

kilometer

kilometer per hour

square kilometer

To convert degrees Celsius (°C) to degrees Fahrenheit (°F) use the following 

formula:

°F = 1.8 x °C + 32.

Sea level: In this report "sea level" refers to the National Geodetic 

Vertical Datum of 1929 (NGVD of 1929)--a geodetic datum derived from a 

general adjustment of the first-order level nets of both the United States 

and Canada, formerly called "Mean Sea Level."
WATER-RESOURCES APPRAISAL OF THE LAKE TRAVERSE 

INDIAN RESERVATION IN SOUTH DAKOTA

By Stephen J. Lawrence 

ABSTRACT

The water resources within the Lake Traverse Indian Reservation consist 

of streams, lakes/ wetlands, and ground water stored in alluvium and glacial 

outwash deposits. Streamflow may cease during dry periods and during the 

winter. Lakes and ponds within the reservation are located predominantly 

within internally drained basins. Evaporation and ground-water recharge 

affect the fluctuations in lake levels and the water quality of the lakes. 

Dissolved-solids concentrations in lakes generally range from 500 to 

10,000 milligrams per liter. Dissolved-solids concentrations in streams 

generally range from 500 to 1,000 milligrams per liter; the water generally 

is suitable for domestic, agricultural, and some industrial use. However, 

nutrient concentrations tend to be greater than natural background concentrations in both lakes and streams, and indicate unidentified sources of 

nutrients that affect the water quality. The development of surface-water 

resources is hindered by a lack of storage capacity within the numerous 

lakes, a lack of sustained streamflow, and a lack of suitable sites for 

construction of reservoirs. Therefore, the ground-water resource remains the 

only source with a potential for development into dependable water supplies 

within the reservation.

Ground-water resources within the Coteau des Prairies, a glacial upland, 

occur within glacial-outwash and alluvial deposits. Recharge and discharge 

points may be present in the Coteau where gravel deposits are within 5 feet 

of land surface. Locally, the sand and gravel deposits in the Coteau may be 

as thick as 70 feet. The water within these sand and gravel deposits 

generally is suitable for most uses; calcium, magnesium, and bicarbonate are 

the dominant ions. Ground water also occurs in sand and gravel deposits 

within the Minnesota River-Red River lowlands. Water in these deposits 

tends to be more mineralized than water in the sand and gravel deposits in 

the Coteau des Prairies. The regional ground-water flow generally is to the 

east in the Minnesota River-Red River lowlands, and to the west in the Coteau 

des Prairies. Additional data are needed to define the ground-water resource 

with sufficient detail to allow knowledgeable development of ground-water 

supplies.

INTRODUCTION

A knowledge of the quantity and quality of both surface- and groundwater resources is an important component of any plan designed to direct the 

economic development of semiarid areas such as South Dakota. Both the Indian 

tribal councils and the U.S. Bureau of Indian Affairs have become keenly 

aware of the importance of water to the Indian tribes of South Dakota. Such 

awareness has been increased by debate about Indian water rights, particularly with respect to the "first in time, first in right" and "use it or lose 

it" concepts in the "appropriation" and "riparian" doctrines of water law, 

and by the need for additional water supplies to support the expanding agricultural base and expanding domestic needs on the Indian reservations. In 

meeting this need for water-resources knowledge, most of the tribal councils 

have completed at least limited studies of the water resources within their 

reservations. Prior to this study, the Lake Traverse Indian Reservation was 

the only reservation in South Dakota without such a study.
This study of the Lake Traverse Indian Reservation in South Dakota 

(fig. 1) brings into a single document both published and unpublished data 

and information regarding the surface- and ground-water resources in the 

reservation. The 105 mi2 of the reservation within North Dakota was not considered in this study. This report focuses on the quantity and quality of 

water, and on distribution of streams, lakes, and water-yielding geologic 

materials to provide knowledge of the water resources and to identify areas 

where data are lacking.

Physiography

Within South Dakota, the reservation occupies a triangular area of 

1,490 mi 2 in the Central Lowlands physiographic province. The reservation is 

located in parts of five counties in South Dakota: Codington, Day, Grant, 

Marshall, and Roberts (fig. 1), and two physiographic divisions: the 

Minnesota River-Red River lowlands and the Coteau des Prairies (Flint, 1955) 

(fig. 2). Each physiographic division occupies about 50 percent of the 

reservation.

The two physiographic divisions have different topographic characteristics. The Minnesota River-Red River lowlands is a nearly flat ground moraine 

that consists of isolated areas of debris left by retreating glaciers (recessional moraine) and glacial meltwaters (outwash) (Koch, 1975). The Coteau 

des Prairies is a plateau of rolling, sometimes rugged, morainal topography. 

This topography was formed by the deposition of rock debris (lateral 

moraines) when Wisconsin ice sheets moved down the James River and Des Moines 

River valleys during the Pleistocene Epoch (Koch, 1975; Lindroth, 1976). The 

result is a hilly topography of moderate to high relief with numerous lakes 

and wetlands. The western face of the Coteau rises 600 ft from the James 

River lowland at a rate of 200 ft/mi, whereas the eastern face rises 800 ft 

from the Minnesota River-Red River lowlands at a rate of 300 ft/mi.

Climate

The climate in the study area is typically continental. Maximum daily 

temperatures average 25 to 31 °C and tend to occur from June through August

(Hodge, 1960). Minimum daily temperatures occur from December through 

February and commonly are less than zero during January. The mean maximum 

daily temperature is 12.8 °C; the mean minimum is -0.6 °C for the 30-year

(1951-80) period of record at Sisseton.

Although the Coteau des Prairies is a prominent upland, there doesn't 

appear to be any orographic effect caused by the Coteau. A majority of the 

precipitation in the area of the reservation occurs during March through 

September. Much of the precipitation is produced by low-pressure areas with 

associated cold fronts (frontal cyclones) moving across the reservation and 

frontal-induced thunderstorms (Hodge, 1960). The average annual precipitation ranges from 20 inches in the eastern part of the reservation to 

22 inches in the southern part (National Oceanic and Atmospheric Administration, 1985). Precipitation tends to be greatest in May, June, and July, 

and least in December, January, and February. Total monthly precipitation 

equal to or greater than 8 inches could occur 5 percent of the time during 

May or June at either Sisseton or Watertown (fig. 3; National Oceanic and 

Atmospheric Administration, 1985). The average annual snowfall ranges from 

32 inches in the northern part of the reservation to 36 inches in the central 

part of the reservation (National Oceanic and Atmospheric Administration, 

1985). Snowfall is greatest in February and March.
98' 97°

oBritton

L_MA_RSHALL_ _ COUNTY 

DAY COUNTY

The boundary of the reservation is , 

described in Article 3, of the Treaty .._ 0 | 

of February 19, 1867 ( 15 Stat. 505). 45 f

S_ _COUNTY_ _ \ 

f COUNTY \

Mi I bank j

Watertown

10 20 30 40 MILES

10 20 30 40 KILOMETERS

100° 98°

45°fo Rapid 

City

43°l _j_____ L _2^

IpO MILES 

100 KILOMETERS

LOCATION MAP

Figure 1.--Location of the Lake Traverse Indian Reservation in South Dakota
^V: :'?-.®;-.V-K-

"T"' 1T "'s"TT11^ ft 'V*

©

 1 1

Webster \ 1 f

\ r i

" ^DI^GTON" ~\ *

\ \

V

Watertown

10______20______30______40 MILES 

10 20 30 40 KILOMETERS

EXPLANATION 

PHYSIOGRAPHIC DIVISION 

James River lowland

Lake Dakota plain

Coteau des Praries

Minnesota River-Red River lowlands

Figure 2.--Physiographic divisions in and near the 

Lake Traverse Indian Reservation.
EXPLANATION

30-YEAR MEAN (WATER 

YEARS 1951-80)

95TH PERCENTILE

Figure 3.--The 30-year (water years 1951-80) mean monthly precipitation and th

for selected sites in and near the Lake Traverse Indian Reser
The predominant wind direction is from the south and southeast during 

the summer, and from the north and northwest during the winter. The average 

annual wind speed is 11 mi/h (Hodge, 1960). The average annual evaporation 

from class A evaporation pans in eastern South Dakota is 46 inches with 

83 percent of that occurring from May to October (Hodge, 1960).

Geology

On the basis of their depositional history, the geologic units within 

the Lake Traverse Indian Reservation are divided into three groups: (1) 

Precambrian crystalline rocks, (2) Cretaceous sedimentary rocks, and (3) 

Alluvium and glacial-outwash deposits and glacial lake sediments (figs. 4 

and 5). Within Marshall County, the Precambrian crystalline rocks (granite) 

are 906 to 1,113 ft below land surface at an elevation of 242 to 407 ft above 

sea level (Koch, 1975). The depth to the Precambrian crystalline rocks is 

not known for much of the Lake Traverse Indian Reservation.

The Cretaceous sedimentary rocks include shale (Pierre, Carlile, and 

Graneros Shales), interlayered beds of limestone (Niobrara Formation and 

Greenhorn Limestone), and sandstone with interbedded layers of shale and 

siltstone (Dakota Sandstone). The Dakota Sandstone directly overlies the 

crystalline rocks. Undifferentiated rock occurs in the northeastern corner 

of the reservation (fig. 4). The individual layers of sedimentary rock 

generally become progressively thinner in an easterly direction (fig. 6).

During the Quaternary period, glacial and post-glacial unconsolidated 

sediments were deposited in the area of the reservation. The following 

description and generalization of the glacial geology of the Lake Traverse 

Indian Reservation is derived from the studies by Flint (1955), Koch (1975), 

and Lindroth (1976).

Glacial deposits or drift within the reservation consist of till, 

glaciofluvial (stream) sediments, and glaciolacustrine (lake) sediments 

(fig. 5). Glacial till is a heterogeneous mixture of clay, silt, sand, 

gravel, and boulders. Landforms such as ground, end, and stagnation moraines 

are commonly associated with glacial till within the reservation. Glaciofluvial sediments include glacial-outwash deposits of sand and gravel 

deposited by flowing glacial meltwaters. Glacial-outwash deposits are 

stratified to semistratified deposits of poorly sorted fine sand and coarse 

gravel. Some glacial-outwash deposits may have till inclusions and may 

overlie alluvium. Glaciolacustrine sediments consist of layered deposits of 

clay, silt, and sand transported into ancient lakes by glacial meltwaters. 

Alluvium along old and recent flood plains and lake beds generally consists 

of semistratified deposits of silt, sand, and gravel, commonly in association 

with humic material.

SURFACE WATER

Important components of a surface-water investigation include a description of the surface-water resources, an analysis of the flow regime including 

peak and low-flow periods, an analysis of storage capacity, and an analysis 

of water-quality data. The goal is to determine if the quantity, timing, and 

location of surface water can meet the demand for beneficial uses of that 

water.

Surface water within the Lake Traverse Indian Reservation includes 

intermittent streams and numerous lakes and wetlands. The reservation is 

located in parts of three major river basins the Missouri, the Souris-RedRainy, and the Upper Mississippi River basins (Seaber and others, 1984). The
98°

^

Watertown

10 -I 20 30 40 MILES

0 10

CRETACEOUS

20 30 40 KILOMETERS 

EXPLANATION

PRECAMBRIAN 

Granite

CONTACT

Pierre Shale 

Niobrara Formation

Carlile Shale

Undifferented sedimentary rocks 

Figure 4.--Bedrock geology in and near the Lake Traverse Indian Reservation.
LAKE I TRAVERSE! 

ERVATIO

_ALL__ _COUNTY_ 11 \ 

t' " COUNTY "" ~^~\

10 20 30 40 MILES

10 20 30 40 KILOMETERS

EXPLANATION 

ALLUVIUM AND GLACIAL-OUTWASH DEPOSITS

GLACIAL-LAKE DEPOSITS

GLACIAL TILL 

CONTACT

Figure 5.--Glacial deposits of Pleistocene and Holocene age in and near 

the Lake Traverse Indian Reservation.
LAKE (TRA

\ RESE

Brllton \

RSHALL COUNTY '. \ 

DAY COUNTY V I

\ ' 

\l

S

O 

WoblUr

\ « 

\ I /

i 

_ _____«| 

JCODINGTONV ~ 

4 \/ 

COTEAU DES PRAIRIES

DATUM IS SEA LEVEL

Base from South Dakota Department of 

Water and Natural Resources, 1975

VERTICAL SCA

10______1

10 15 20 KIL

Figure 6.--Geologic section across the northern part of the Lake Traverse 
Big Sioux and James Rivers are tributaries of the Missouri River and drain 

578 mi 2 of the Lake Traverse Indian Reservation. In most years, about 

324 mi 2 of the basins of the Big Sioux and James Rivers are noncontributing, 

draining internally. However, this area may contribute runoff to the Big 

Sioux and James Rivers during extremely wet periods. The headwaters of the 

Big Sioux originate within the reservation with most of the headwater streams 

flowing intermittently from the east side of the basin (fig. 7). The Big 

Sioux River is hydraulically connected to surficial glacial outwash and 

alluvial deposits throughout its length. Although primarily a gaining 

stream, the river also is a losing stream in some reaches. The Big Sioux 

River discharges into the Missouri River at Sioux City, Iowa.

Most lakes and ponds in the reservation are located in the noncontributing parts of the Big Sioux River and James River basins (fig. 8). Many 

lakes lie within closed basins and vary in size and depth with time because 

of vagaries of weather; however, a significant number of lakes are hydraulically connected to and sustained by glacial-outwash aquifers. Long-term 

records of lake levels are available for only three lakes in the noncontributing area; however, since 1982 the South Dakota Department of Water and 

Natural Resources, Division of Water Rights, has collected lake-level data 

for numerous lakes in the noncontributing area. No substantial streams are 

located in this area.

Because the Big Sioux River is important from an irrigation and water 

rights standpoint in eastern South Dakota, six of the eleven streamflowgaging stations located within the reservation are in the Big Sioux River 

basin. As of 1986, two of the gages (sites 8 and 13) provide a continuous 

record of streamflow; the other four have been discontinued (table 1).

About 414 mi 2 of the reservation (fig. 9) is drained by headwater 

streams of the Red River of the North, which is located north of the study 

area in the Souris-Red-Rainy River basin. The eastern part of this area of 

the reservation typically is almost flat; surface runoff flows to and is 

stored in numerous sloughs before flowing into Lake Traverse. Lake Traverse 

is a natural lake, 1 mi wide by 17 mi long, situated in a trough along the 

Minnesota-South Dakota border. Although the lake is natural, a dam and 

control structure has increased the storage capacity to 137,000 acre-ft with 

a surface area of 11,500 acres at maximum pool (South Dakota Department of 

Water and Natural Resources, 1975). Mud Lake, downstream from Lake Traverse, 

is an additional flood-control reservoir in the basin. The channelized Bois 

de Sioux River flows north from the Mud Lake dam at White Rock and into the 

Red River of the North at Wahpeton, N. Dak., about 36 river miles north of 

White Rock. The streamflow-gaging station at White Rock (fig. 9) is the only 

station in the Red River of the North basin within the reservation that has a 

continuous streamflow record, albeit regulated flow. Small headwater streams 

of the Wild Rice River originate in and flow northwestward from the north end 

of the Coteau des Prairies. The Wild Rice River subsequently discharges into 

the Red River of the North.

The Little Minnesota River drains 498 mi2 of the Upper Mississippi River 

basin (fig. 10). The headwaters of both the Little Minnesota River and its 

major tributary, the Jorgenson River, are located within the reservation. 

The headwaters of both rivers are sustained by springs originating in 

glacial-outwash deposits in the Coteau des Prairies. These streams flow down 

the steep eastern escarpment of the Coteau and across the reservation within 

the Minnesota River-Red River lowlands to Big Stone Lake, which is south of 

Lake Traverse and outside of the reservation. The streamflow-gaging station 

near Peever (fig. 10 and table 1) provides continuous discharge records for 

the Little Minnesota River.

10
\

97°I5' 

I

LAKE TRAVERSE INDIAN

RESERVATION

O

 ^4/1

EXPLANATION

BOUNDARIES 

^ » Drainage Basin

 . . Drainage Subbasin

STREAMFLOW-GAGING STATION 

Number refers to stations in 

tables I and 2

Watertown

8 10 MILES

0246 8 10 KILOMETERS

Figure 7.--Contributing drainage area of the Big Sioux River basin upstream 

from confluence with Mud Creek and location of streamflow-gaging stations 

in the contributing part of the basin in and near the Lake Traverse Indian 

Reservation.

11
\ LAKE TRAVERSE INDIAN 

RESERVATION 97°I5' 

I

SO «0 MILE

2O SO «0 KILOKCTCRS

45°30' .-

EXPLANATION

NONCONTRIBUTING 

DRAINAGE AREAS

Big Sioux River basin 

James River basin

BOUNDARIES 

Drainage Basin

Subbasin boundary between 

noncontributing and contributing drainage areas

V~

10 2O MILES

10 20 KILOMETERS

V

Figure 8.--Noncontributing drainage areas of the Big Sioux and James River 

basins, and location of selected lakes in and near the Lake Traverse 

Indian Reservation.
98° NORTH DAKOTA

LAKE TRAVER

RESERVA

r

\ \ v- M i / -\

 \ L4/^-^^-

10 20 KILOMETERS

K) 20 JO 40 MILE!

O 10 2O 3O 40 KILOMETERS

EXP

...DRAINA

 DAM

J STRE

Nu

tab

Figure 9.--Drainage area of the Souris-Red-Rainy River basin and location of 

. stations in and near the Lake Traverse Indian Reservation.
l_

IO M W 40 KILOHCTtm

97° 

I

LAKE TRAVERSE

INDIAN RESERVATION

A 45°45

EXPLANATION 

. DRAINAGE-BASIN BOUNDARY

A5 STREAMFLOW-GAGING STATIONNumber refers to stations in 

tables I and 2

i . Whipgie- ., I i s*~\o S^ Impassable 

|C7-^ . Marsh 

1 i JTDry wood 

Jc( Lakes

 ^ /

s ,/___._

I 29 MILES

l 20 KILOMETERS

Figure 10.--Drainage area of the Upper Mississippi River basin and location 

of streamflow-gaging stations in and near the Lake Traverse Indian 

Reservation.

14
Table 1. Streamflow-gaging stations operated bv the U.S. Geological Survey

in and near the Lake Traverse Indian Reservation

Drainage

Site

number

1

2

3

4

5

6

7

8

9

10

11

12

13

Station

number

05050000

05051650

05289950

05289985

05290000

05290300

06479200

06479215

06479230

06479240

06479260

06479350

06479438

Station

name

Bois de Sioux River near White Rock

La Belle Creek near Veblen 1

Little Minnesota River tributary

at Sisseton2

Big Coulee Creek near Peever 1

Little Minnesota River near Peever

North Fork Whetstone River tributary

near Wilmot

Big Sioux River near Ortley2

Big Sioux River near Florence3

Big Sioux River tributary near Summit

Big Sioux River tributary No. 2

near Summit 2

Big Sioux River tributary No. 3

near Summit 2

Soo Creek tributary near South Shore2

Big Sioux River near Watertown4

area

( square

miles)

1,160

236

447

.96

53.8

638

1.27

.26

6.61

1.56

1,007

Period of

record

(water

years)

1942-86

1970-79

1940-81

1970-79

1956-68

1984-86

1956-67

1956-73

1956-78

1970-79

1973-86

J Gaging station established at end of water year 1986. 

2 Crest-stage gage, only peak flows recorded. 

Contributing drainage area is 67.9 square miles. 

Contributing drainage area is 228 square miles.

Surface-Water Quantity

Streams

The purpose of this section is to provide a brief analysis of the 

quantity, timing, and dependability of streamflow within the Lake Traverse 

Indian Reservation. Logarithms of annual flood peaks and the minimum 7 and 

15 consecutive days of flow in each month were fit to a Pearson Type III 

distribution to estimate the frequency of high and low flows. The percentage 

of time a daily flow was less than a certain value during a given month also 

was computed for several gaging-station records.

Streamflow for the Big Sioux, Little Minnesota, and Bois de Sioux Rivers 

has significant seasonal trends, with streamflow generally being greatest 

from March through June (fig. 11). Most of the annual runoff occurs during 

this period and is caused by melting of the winter snowpack and by spring 

rains. The smallest discharges occur from December through February not only 

because precipitation is less, but also because the streams are ice-covered 

and snow is the principal form of precipitation during this time.

The mean monthly discharge of the Little Minnesota River near Peever is 

less than 0.08 ft 3 /s for 10 percent of the time from December through 

February, whereas the mean monthly discharge at the Bois de Sioux River near 

White Rock and the Big Sioux River near Watertown is less than 0.01 ft 3 /s.

15
Reservation.

at three streamfl

o

cw 

cwh1 -

CW 

to

rt

O

h1 -

^

a

(D

*

rt

(I)

0^

?r

2 Traverse Indian

Figure 11.--Statist

to °OA

0 *

g

3 * 

o ^

rt

p. ^ 

h1 -

to -IT

O "^

OP 

0> <^

CL

i-h

o "fc.

h^r* ^

(D

Deriod ofrecord

DISCHARGE, IN CUBIC FEET PER SECOND 

_ c

0 0 C

1 "I

1

j C

I s

OD

in

0

~m

>m

li

m

o

0

DISCHARGE, IN CUBIC FEET PER SECOND 

> _ c

, 0 _ 0 C

1

 IH

j C

J 5

1 

H 

m

. z

- z 

1m 

in

^

<

z

m 

m

DISCHA

. 0 

 

 

mm

i

----

 BpHlH
The median of the mean monthly discharge for the Little Minnesota River near 

Peever ranges from 0.91 ft 3 /s in January to 100 ft 3 /s in April. The median 

for the Bois de Sioux River near White Rock ranges from less than 0.01 ft 3 /s 

in December through February to 50 ft 3 /s in May; the median for the Big Sioux 

River near Watertown ranges from 0.04 ft 3 /s in February to 40 ft 3 /s in April 

(fig. 11). The relatively small runoff amount from the Big Sioux River basin 

is due to the smaller contributing drainage area. Streamflow at the gaging 

station on the Bois de Sioux River near White Rock is regulated by releases 

from Mud Lake.

Peak-flow data are available for several gaging stations located within 

the Big Sioux River basin and one station located within the Little Minnesota 

River basin. Peak-flow data are used to estimate the probability of occurrence of peak flows of a given magnitude. Peak flows expected to occur at 

stations within the Lake Traverse Indian Reservation and their recurrence 

intervals are given in table 2. Because peak-flow data are based on short 

periods of record (10 to 23 years)/ the estimates of flood frequency have 

large uncertainties/ particularly at the longer recurrence intervals.

Cumulative runoff statistics are given in figure 12. These graphs 

represent the cumulative monthly runoff that is not exceeded/ on the average/ 

25/ 50/ and 75 percent of the time. This is a hypothetical flow condition 

that is unlikely to occur in any given year.

The cumulative runoff at the end of a water year in which the median 

flow occurred each month is 0.91 inch for the Little Minnesota River near 

Peever/ 0.62 inch for the Bois de Sioux River near White Rock, and 0.16 inch 

for the Big Sioux River near Watertown. The Little Minnesota River has the 

greatest cumulative runoff of all three continuous-record gaging stations 

because of the larger drainage area and greater ground-water flows from the 

Coteau des Prairies to the headwaters of the Little Minnesota and Jorgenson 

Rivers. Except for the 25th-percentile flows, the cumulative runoff for the 

Bois de Sioux River near White Rock is about the same as for the Little 

Minnesota River near Peever. The 25th-percentile flows represent runoff 

during dry periods when releases from Mud Lake are minimal. The Big Sioux 

River near Watertown has cumulative runoff values that are smaller than those 

for the Little Minnesota or the Bois de Sioux Rivers. These smaller values 

result from a smaller quantity of runoff caused by a smaller contributing 

drainage basin and smaller ground-water flows.

A knowledge about periods of sustained flow/ particularly low flows, is 

important to water-pollution-control efforts, water-supply forecasting/ and 

reservoir operations. Therefore/ an analysis was conducted to determine the 

minimum discharge expected for 7 and 15 consecutive days in a given month 

once every 10 years. These discharge values are known as the 7Q10 and 15Q10 

flows/ respectively/ and are often used on an annual or seasonal basis by the 

State and the U.S. Environmental Protection Agency to establish minimum 

instream water-quality standards for streams receiving treated wastewater. A 

7Q10 of 0.1 ft 3 /s or less can be expected for the Big Sioux River near 

Watertown during June/ October, and November; and a 7Q10 of zero can be 

expected from July through September and from December through March 

(fig. 13). The Little Minnesota River, with its larger contributing drainage 

area/ has a slightly greater sustained flow than the Big Sioux River near 

Watertown, but a similar flow regime. Records for the Little Minnesota River 

near Peever and the Big Sioux River near Watertown indicate ground-water 

inflow during the fall due^. in part to recharge by irrigation water. In 

contrast, the Bois de Sioux River near White Rock has 7Q10 and 15Q10 flows 

nearly an order of magnitude smaller than either the Little Minnesota or the 

Big Sioux Rivers. This is probably due to the effect of the controlled flow 

out of Mud Lake.

17
Table 2. Magnitude and recurrence interval of instantaneous peak flow at 

CD

stations in and near the Lake Traverse Indian Reservation

[Source: Hoffman and others, 1986]

Discharge, in cubic fee

Period for recurrence interval, 

of annual exceedance probabi

analysis 

Site Station Station name (water Years: 2 5 

number number years) Percent: 50 20

3 05289950 Little Minnesota River 1970-79 80 208 

tributary at Sisseton

7 06479200 Big Sioux River near Ortley 1956-68 141 394

10 06479240 Big Sioux River tributary 1956-73 8.9 25

10 

10 

336 

655 1

41 

11 06479260

No. 2 near Summit

Big Sioux River tributary 

No. 3 near Summit

1956-78 94 331 591 1

12 06479350 Soo Creek tributary near 

South Shore

1970-79 44 129 222 

13 06479438 Big Sioux River near 

Watertown

1973-85 569 1,350 2,100 3
1.840

NJ 

UJ

UJ

UJ 1,835

IS)

UJ

>

O

CD 1,830

hUl 

UJ

UJ 

>

UJ

_1

UJ

1,825

1,820

1,815

4-0

I/) 

Ld

T. 

U

_J

20

 DATA POINT FOR BUFFALO LAKES +

+ ESTIMATED DATA

D DATA POINT FOR ENEMY SWIM LAKE

o NO DATA

CONNECT LINES INDICATE DATA TRENDS

X 

X

X

R

X 

X 

X 

X

X

x

X 

X

X

X 

X

X

J

X 

X 

X 

X 

X

r 

X 

X

'

/

^

X

r

X

X 

X 

X

X

rX

X 

X 

X

x

7

X 

X 

X 

X

^^ ^^

QQ

oo

X

X 

X 

X

«

<5

QQ 

OO

X 

X 

X

r 

X 

X 

X 

X 

X

rX 

X 

X 

X 

X 

X

r 

X 

X 

X 

X

X 

X

X 

X

x

x

X 

X

X 

X

X

X 

X

X

x

X 

X 

X

r 

X 

X 

X 

X 

X

r 

X 

X 

X 

X

X

X

X 

X 

X

X 

X

X

X 

X 

X 

X

x

X

X

X 

X 

X

x

x

X 

X

x

X 

X

x

X 

X 

X

WATER YEAR

Figure 14.--Lake levels and corresponding total rainfall at Sisseton 

Estimated data produced by regressing data for Buffalo Lakes agains

(Source: State Lakes Preservation Committee, 1977.)
SPECIFIC CONDUCTANCE pH DISSOLVED OXYGEN TOTAL ALKALINITY

1U,UUU

cr 

u

UJ(/>

CENTIM PERCELSIU REES 

"o 0 o

zu

UJQ

Is

(/! 

rx

u

2

; 153 277 121 :

1 1 i

ilj

i

.

.

-

'

.

'

"

.

i^

12

10

H

D 8

0

1 < 6 h4

2

n

92 217 122

_

J

i

_

"

_

f,1 -

_

-

JU

o: 

u

H

cc 25 

u

Q.

MILLIGRAMS KJ_> tn o

Z

z"

o 10

1 

cr

z

u 5

U

z

o

u

rt

117 269 14-9

-

-

(

i

(

«

t

-

T

D.UUU

ce 

u

H

_j

u I- 000

Q. LJ

If

du 100

ZD

-U 

Z-J

a< 10

^

u

u

z

o

u

 58 156 98 

.

ii 

'. E

- i

]E

i

:

^

3 c

i

3 :

-

;

.

1

100 u u - i 

123 123 123 123

SITES SITES SITES SITES

TOTAL DISSOLVED SOLIDS

3,UUU

cr 

u

t

o:

u

Q.

CO

2

cr 

55 1,000

2

z 

z"

o

l^r

cr hz

u

u

z

o

u

inn

 18 32 14

 

: I

 R "

r

1

T

.

i 1 1 

I,UUU

ce 

u

t

ce

u

Q.

10

2 

ce

2 100

z 

z"

o

^

ce1-

z

UJ

u

z

o

u 

m

: 56 97 41 ;

i '

\[](

, i

I" '

_

:

1 1

.

EXPLANATION

45 -- NUMBER OF SAMPLES 

TOTAL CALCIUM t --MAXIMUM

-- 75TH PERCENTILE

-- 50TH PERCENTILE (MEDIAN)

-- 25TH PERCENTILE

-- MINIMUM

 DETECTION LIMIT

 STATE SURFACE WATER QUALITY 

STANDARD FOR DOMESTIC 

WATER SUPPLY

SITES / j i ^ j

1 Big Sioux River near Watertown 

SITES SITES (06479438)

2 Little Minnesota River near 

Sisseton (4539400965730)

3 Little Minnesota River near 

Peever (05290000)

Figure 15.--Streamflow quality at three sites in and near the Lake Traverse 

Indian Reservation. (Source of data: South Dakota Department of Water 

and Natural Resources.)

24
Lakes

Most lakes and ponds within the reservation are located within the 

noncontributing part of the Big Sioux River and the James River basins. 

Because of large surface areas, shallow depths, and effects of evaporation 

and ground water, the volume of water in storage within the lakes is neither 

sufficient nor predictable enough for major development of dependable water 

supplies. Even though the total storage in 1975 was estimated to be at least 

205,000 acre-ft (State Lakes Preservation Committee, 1977), no one lake has a 

sufficient storage capacity or a dependable inflow of water to make it 

economically feasible for major development (table 3).

The lakes are located within basins that may differ greatly, even from 

adjacent basins, in terms of geology, ground-water inflow, and inflow-outflow 

relations. Some of these lakes, such as Bitter, Hillebrands, and Isabella 

(fig. 8), are nearly or completely closed systems within glacial till 

(table 3). The hydrologic cycles of these lakes are dominated by surface 

runoff and evaporation. Other lakes, such as Pickerel, Buffalo, and Enemy 

Swim (fig. 8), are hydraulically connected to gfacial-outwash aquifers and 

probably are regulated indirectly by the effect of rainfall on ground-water 

levels (fig. 14).

Surface-Water Quality

On the basis of an analysis of data from the South Dakota Department of 

Water and Natural Resources, the surface-water quality, with respect to 

inorganic constituents, in the Lake Traverse Indian Reservation is such that 

the water probably is suitable for domestic, recreational, industrial, and 

irrigation uses (U.S. Environmental Protection Agency, 1976, 1986a, b, c).

Streams

Data for pH, dissolved oxygen, fecal coliform bacteria, total alkalinity, total nitrate, total ammonia, and total orthophosphate appear to be 

similar at the Bois de Sioux River (table 4), the Little Minnesota River, and 

the Big Sioux River (fig. 15). Occasionally, pH values may not be within the 

surface-water quality standard of 6.5 to 9.0 units for domestic water 

supplies, nitrate concentrations may exceed the standard of 10 mg/L (milligrams per liter) as nitrogen, and total dissolved solids may exceed the 

standard of 1,000 mg/L (South Dakota Department of Water and Natural 

Resources, 1986). The large values of pH and concentrations of dissolved 

oxygen indicate that algal blooms occasionally may occur in all three rivers. 

Rapid rates of photosynthesis produce a supersaturation of dissolved oxygen 

and more alkaline conditions as algae take up carbon dioxide and release 

oxygen. The smaller concentrations of dissolved oxygen also may occur as a 

result of algal blooms as respiration, rather than photosynthesis, occurs 

during the night, or when ice cover and low-flow conditions prevail and 

oxygen demand for decomposition within the sediments is large. Occasional 

large concentrations of fecal coliform bacteria, total nitrate, total 

ammonia, and total orthophosphate indicate probable contamination from either 

feedlots, septic tanks, or sewage lagoons. Unfortunately, there are no fecal 

streptococcus bacteria data available to determine whether the fecal coliform 

bacteria are of human origin. The fecal coliform bacteria concentrations at 

times may exceed State standards for immersion recreation (200 colonies per 

100 milliliter from May 1 to September 30) and limited contact recreation 

(1,000 colonies per 100 milliliter from May 1 to September 30).

21
Table 3. Physical characteristics of selected lakes in and 

near the Lake Traverse Indian Reservation

[Source: State Lakes Preservation Committee, 1977. 

 indicates data were not supplied by source]

Lake

Cottonwood

Still

Surface area

Acres Square 

miles

422

416

Codington

0.66

.65

Depth

Average

County

2

2

(feet)

Maximum

6

Watershed 

area 

(square 

miles)

7.62

68.28

Day County

Blue Dog 

Bitter 

Enemy Swim 

Hillebrands

Lonesome

Pickerel

Spring

1,498 

4,173 

2,144 

666

102

954

998

2.34 

6.52 

3.35 

1.04

.16

1.4

1.56

6 

2 

10 

5

5

20

4

8 

26

8

43

115.33 

38.95 

34.86 

2.66

6.15

26.82

5.58

Grant County

Twin 205 0.32

Marshall County

1.24

Buffalo, North

Buffalo, South

Clear

Greys

Isabella

Long

Mud

Piyas

Red Iron, North

Turtlefoot

Drywood, North

Drywood, Middle

Drywood, South

Hurricane

Oneroad

Owl

Tahana

Traverse

Whitestone

265

1,685

1,094

141

70

294

166

1,280

173

122

914

2,133

192

326

288

179

41

10,600

262

0.41

2.63

1.71

.22

.11

.46

.26

2.00

.27

.19

Roberts

1.43

3.33

.30

.51

.45

.28

.07

18.12

.41

10

7

12

4

3

4

4

3

7

3

County

6

7

4

6

4

4

4

7

8

12

12

20

10

5

9

10

11

10

10

6

12

7

9

12

16

28.15

26.22

58.34

1.59

1.26

8.79

1.36

4.59

43.75

.77

5.67

(M

1.16

6.08

6.61

.61

.11

1,139.07

1.15

1 Watershed area grouped with North Drywood Lake,

22
6T

INCHES IN RUNOFF, CUMULATIVE 

w

rr 

(- o

(A

o w 

it) rt 

0)

o rt C H- 

»- §1w 

to

rt M» 

H. 3

ft) 0) 

H H Z Z 

 « O 

ni rn n n z z r r 

ft n 

" 2 H - 3

3 3 

rt O 

3* 0) 

(D

it) O H 

*d «> 

0>

H W 

H. 3 o a O 3 H CD 

<D W O O O 1 M <J 

a co 

rt Q) H. 

rt o 

3 

rt 

(W 

0)

rj n u

tf * 5 -< < n 
BIG SIOUX RIVER NEAR WATERTOWN 

( WATER YEARS 1972-86 )

UTTLE MINNESOTA RIVER NEAR PEEVER 

( WATER YEARS 1939-81)

BOIS DE SIO

( WA

o

o 

(J

UJ 10

o:

UJ

Q.

UJ 

UJ

u.

y e

CO

u 

? 4.

o 

o:

u 

I/}

o

- a 7oio

m 15Q10

rll 

o^^ A A 

Figure 13.--The 7-day, 10-year (7Q10) and 15-day, 10-year (15Q10) minimum discharges 

record at three streamflow-gaging stations in and near the Lake Traverse Indian 
CONCENTRATION, IN MILLIGRAMS PER LITER CONCENTRAT

c

-»

00 

H M

m

00

u)

0 - C

I _» - o c

__, | i . w

 III °!

 "Ill -si

 i i i . y

3 3

ft^

°°00

ZO

o3

cn^ m>

o zC

00 

H M

m

00

to

 

 

* 

CONCENTRATION, IN MILLIGRAMS PER LITER CONCENTRAT

to

tn

-»

00

H to

00

_»

00

H M

m

00

u>

H II -5

 1 1 1 IN

 H 1 1 io

...... 1 . . ,..,..!

COLONIES PER 100 MILLILITERS

_ c

_. 0 C

_ o o c

_ 0 O 0 C

o o a o c

11111

 1 1 ) ~~*

1 *

1 | | | . ol

1 ' ' vD

1 1 1 1 . U>

1 1 1 0

. ...,.i . . . .....i . . . .....i . . . .....i . ......

>O

00-|

:?r~

O-o

 oo

OT3

CO

COX) C

00

33ii3

corn

>n

n> 

nr

2o

 ** io

73^

00 

H M

rn

00

 

 

 

CONCENTRAT

c c

_»

00

H M

00

u>

3 

3 f

3

1 
Table 4. Summary of water-quality data for the 

Bois de Sioux River near White Rock

[Number of analyses = 15. Results in milligrams per liter except as

indicated; °C, degrees Celsius; JTU, Jackson turbidity units;

CaCO3/ calcium carbonate; N, nitrogen; P, phosphorus]

Property or constituent Maximum Mean Minimum

Specific conductance (microsiemens 2,860 1,360 754

per centimeter at 25 °C)

pH (units) 8.4 7.7 7.4

Temperature, water (°C) 26.9 15.8 0.6

Turbidity (JTU) 130 90 8

Dissolved oxygen 11 7.2 2.6

Biochemical oxygen demand 15 6.6 2.0

Total coliform bacteria (colonies 3,300 800 200

per 100 milliliters)

Fecal coliform bacteria (colonies 400 200 20

per 100 milliliters)

Hardness, total as CaCO3 1,600 670 350

Hardness, noncarbonate as CaCO3 520 177 18

Calcium, dissolved 300 130 68

Magnesium, dissolved 210 86 47

Sodium, dissolved 140 64 25

Sodium-adsorption ratio 1.6 1.0 0.6

Potassium, dissolved 21 14 8

Bicarbonate 480 330 220

Sulfate, dissolved 1,400 510 200

Chloride, dissolved 35 17 6.8

Fluoride, dissolved 0.6 0.3 0.2

Silica 34 18 7.7

Dissolved solids, residue at 180 °C 2,370 1,020 529

Nitrate, dissolved as NO3 5.8 2.9 1.0

Un-ionized ammonia as NH4 1.3 0.3 <0.01

Orthophosphate, dissolved as P 0.55 0.33 0.15

Boron, dissolved (micrograms per liter) 320 220 90

Iron, dissolved (micrograms per liter) 950 120 30

Manganese, dissolved (micrograms 310 100 10

per liter)

26
The Big Sioux River near Watertown has somewhat less mineralized water 

than the Little Minnesota River near Peever and near Sisseton, which may be a 

result of the glacial-outwash sediments that dominate the Big Sioux River 

basin. The influence of surficial outwash deposits is greatest in the 

headwaters of the Little Minnesota River and minimal for the Bois de Sioux 

River. Specific-conductance values and calcium, magnesium, sodium, and 

dissolved-solids concentrations generally are smaller in the Big Sioux River 

than those at the other two stations. The Little Minnesota River near Peever 

has the narrowest range of specific-conductance values and calcium, sodium, 

and magnesium concentrations. The reason for this is unknown. Although 

specific conductance and dissolved solids can give a general indication of 

water quality, a more specific description of surface-water quality cannot be 

given because data for chloride, sulfate, potassium, trace metals, and 

organic compounds are not available for the stations in the reservation.

Lakes

Because of the considerable variation in the geology and other factors 

governing the hydrologic cycle of lakes within the reservation, a variety of 

water-quality regimes occur. A listing of lakes divided into general waterquality categories by dissolved-solids concentrations is given in table 5. A 

detailed summary of the water quality of four lakes from three of the four 

categories in table 5 is given in figure 16. There were not enough data to 

adequately summarize other lakes given in table 5, particularly for lakes 

with dissolved-solids concentrations ranging from 500 to 1,000 mg/L.

Bitter Lake, just west of the reservation, was used as a representative 

of the group of lakes with dissolved-solids concentrations greater than 

4,000 mg/L because Bitter Lake had the most data for lakes within that group. 

This group of lakes is located within basins composed of glacial till; therefore, the lakes have little ground-water inflow and have large losses of 

water from evaporation. The water quality of Bitter Lake is characterized by 

a large concentration of dissolved solids due primarily to the concentration 

of solutes within the lake by evaporation (fig. 16). Maximum concentrations 

of calcium, magnesium, sodium, sulfate, chloride, and dissolved solids were 

measured in February when the lake was covered by ice. Large concentrations 

of dissolved solids may occur during winter ice cover when the formation of 

ice pulls water molecules into the ice layer, leaving dissolved ions in the 

water, which progressively concentrates minerals within the unfrozen part of 

the lake. Water with a large concentration of dissolved solids has a 

freezing point less than 0 °C.

Because of the large concentration of dissolved solids in the lake, it 

is probable that precipitation of calcium carbonate is occurring. The small 

calcium and alkalinity concentrations relative to magnesium, sodium, and 

chloride concentrations tend to support this hypothesis. The water quality 

within Bitter Lake is, therefore, dominated by magnesium sulfate (fig. 16). 

It seems likely that similar reactions and processes occur to varying degrees 

within Hillebrands Lake and Lake Isabella. Water in Bitter Lake is not 

suitable for domestic uses because of taste and cathartic effects; for agricultural uses because of salt buildup in soils that results in a detrimental 

effect on plants and because of excessive constituents that may have a 

possible unhealthy effect on livestock; and for most, if not all, industrial 

uses because of mineral buildup in pipes, and corrosion of machinery.

27
SPECIFIC CONDUCTANCE TOTAL ALKALINITY TOTAL DISSOLVED SOLIDS

5,000

cr

UJ IUJl"

P 3 

BB

ZUJ 

UJQ

2^

 7 22 18 7

1,000 :

100

234 

SITES

13 21 11 13

^cr 1,000 - ,-L, 

du

o<P u

< I/I

UJ 

U

z 

o 

u

100

T

1234 

SITES

1UU,UUU

cr

UJ

t

cr

UJ

a.

< 10,000 

cc

Ii

i

z

z" 

9. 1,000

cr

1 _

CONCENl

0 o

11 11 11 13 I

1 :

gU :

: :

t

_ _ _ n ..

.

: *"? :

1234

SITES

DISSOLVED CALCIUM DISSOLVED MAGNESIUM

EXPLANATION

45 -- NUMBER OF SAMPLES 

-- MAXIMUM

1,UUU

cr

UJ

t

cr

UJ

a.

t/i

< 100

cr

e>

z

z"

2 10

cr Iz

UJ

u

z

o

u

12 11 6 17 :

.

"

I

- H U -

EV J^l \ Ji. il R =

: :

.

cr

UJ

t

cr

UJ

a.

(/)

< 1,000

o:

(J

z

z"

2 100

cr Iz

UJ

U

z

o

u

4 St

: 12 11 6 17 :

 - * ' -

"

~

?

-

.

«

- :

I

 ± -:

: , 9 '' 

 T 4s

i

- - 75TH PERCENTILE

- -- 50TH PERCENTILE (MEDIAN)

r -- 25TH PERCENTILE

. -- MINIMUM

 STATE SURFACE WATER OUALIT

STANDARD FOR DOMESTIC

WATER SUPPLY

1 .u 

1234 1234

SITES 

Bitter Lake

SITES SITES 2 Enemy Swim Lake

3 Pickerel Lake

4 Lake Traverse

Figure 16.--Water quality of four lakes in and near the Lake Traverse Indian 

Reservation. (Source of data: State Lakes Preservation Committee, 1977.)

28
CONCENTRATION, IN MILLIGRAMS PER LITER CONCENTRATIO

to 

vo

c

-»

H 

m 

to u

 f^

c c

to to

H m00 LJ

K,

C

H 

rn

c c

H 

m ,

I S - c

H 1 h-

 1 II 

CONCENTRATION, IN MILLIGRAMS PER LITER

3

i 2 - c

LIMITED DATA to

1 I _____ _ IO 

1 1 o

 1 | ( * -J

 I 1 1 s

CONCENTRATION, IN MILLIGRAMS PER LITER

3 

 c

LIMITED DATA to

 OH 3

CONCENTRATION, IN MILLIGRAMS PER LITER

3

; S - c

LIMITED DATA M

" ]|

r~~" n 

 1 Ih* °>

; ?

10 M -*

ZO

Oo ~l

^ m u

50 -fr\

>

^

j?< to to

cno r{

5> to u

2

2 K

O Z

>

nr ~*

oH W

2° n u

m z

3

too

i!

tol° oo to

TO =j C

00

) 

_ 

CONCENTRATIO

_ 

0 

 JJ 

l] 

ff'1 

CONCENTRATIO

_ 

O 

 CD 

1 

CONCENTRATIO

_ 

0 

 HU 

MD 
Table 5. Lakes in and near the Lake Traverse Indian Reservation 

grouped by median concentrations of dissolved solids

Lakes with median dissolved-solids concentration less than 500 milligrams per 

liter

Blue Dog

Hurricane

Enemy Swim

Pickerel

Oneroad

North and South Red Iron

Lakes with median dissolved-solids concentration between 500 and 

1,000 milligrams per liter

Long

Clear

Whitestone

North and South Buffalo

Greys

Mud

Lakes with median dissolved-solids concentration between 1,000 and 

4,000 milligrams per liter

Piyas

North and South Drywood

Tahana

Turtlefoot

Traverse

Lakes with median dissolved-solids concentration greater than 4,000 

milligrams per liter

Bitter

Hillebrands

Isabella

30
Water-quality data for Lake Traverse are in many respects more similar 

to data for Bitter Lake than to data for Enemy Swim or Pickerel Lake because 

of the limited hydraulic connection of Lake Traverse with ground water 

(fig. 16). Lake Traverse is dominated by calcium, magnesium, and sulfate, 

and has more calcium and less sulfate than does Bitter Lake. Even though 

some precipitation of calcium carbonate probably occurs in Lake Traverse, 

particularly during droughts, it is not a dominant process within the lake.

The water quality of Pickerel and Enemy Swim Lakes provides a marked 

contrast between the Bitter Lake and Lake Traverse water-quality regime, and 

represents the quality of lakes with a dissolved-solids concentration less 

bhan 500 mg/L (table 5). These lakes have the least mineralized water of 

Lakes within the reservation (fig. 16). Pickerel and Enemy Swim Lakes are 

nydraulically connected to a glacial-outwash aquifer, and their water levels 

reflect the water table of that aquifer. Therefore, levels of these lakes 

should rise and fall independently of evaporation. According to the South 

Dakota Department of Water and Natural Resources (1986) , Pickerel and Enemy 

Swim Lakes (Leap, 1972) are hydraulically connected to areas where the Coteau 

Lakes aquifer is thick and may also be recharge areas for the aquifer. Water 

quality in these lakes probably reflects the water quality of the aquifers 

sustaining them.

Concentrations of dissolved nitrate, organic nitrogen, and phosphorous 

fluctuate greatly in all four lakes. It is difficult to establish a reason 

for this fluctuation without additional data and interpretation. However, 

because most of the lakes tend to be sinks for nutrients, nutrient concentrations would be expected to be greater than those in streams. Feedlots, 

septic tanks, and agricultural fertilizers have been identified as sources of 

nutrients for many of these lakes (State Lakes Preservation Committee, 1977). 

Therefore, lakes within the reservation tend to be eutrophic to varying 

degrees, some to the extent that nuisance blooms of algae are common, 

requiring remedial measures to eliminate blooms and preserve the esthetic 

quality of the lakes (State Lakes Preservation Committee, 1977).

With the exception of a few lakes, surface water within the reservation 

generally is suitable for domestic, agricultural, and industrial uses. 

Significant development of this resource is limited by the lack of dependable 

quantities and a lack of potential storage capacity. The potential uses of 

lakes within the reservation may be impaired because of large nutrient 

concentrations and subsequent algal blooms, which degrade the water quality 

and the esthetic quality of the lakes. Additional data and interpretation 

are needed to determine the hydrologic processes and sources of nutrients 

affecting water quality of the lakes. Bitter Lake and Lake Hillebrands are 

potential sites for studying hydrogeochemical processes and controls of those 

processes within a closed-basin lake.

GROUND WATER

Even though ground water is being used by the city of Sisseton and by 

individual farmers and homeowners, the distribution, quantity, and quality of 

ground water in the reservation is not well known. Therefore, in order to 

determine whether sufficient water of acceptable quality is available for 

agriculture and housing developments, an analysis of the ground-water 

supplies and hydrogeology is needed. The following narrative will summarize 

what is known about the ground-water resources in the reservation.

31
Hydrogeo1oqv

The substantial differences in physiography within the boundaries of the 

reservation also are paralleled by differences in hydrogeology in the 

Minnesota River-Red River lowlands and the Coteau des Prairies. Within the 

Coteau, deposits of sand and gravel, commonly containing interbedded layers 

of till, occur at various depths from the land surface to depths of 230 ft or 

greater below land surface. According to Koch (1975), several aquifers can 

be delineated within the Marshall County part of the reservation. These 

aquifers include the Coteau Lakes, Marday, and Eden aquifers. The Prairie 

Coteau, Eastern Lakes, Lonesome Lake, and Big Sioux aquifers also underlie 

the Coteau des Prairies. Koch (1975) identified an additional aquifer, the 

Veblen aquifer, in Marshall County that extends from the northeastern toe of 

the Coteau north into North Dakota and east and southeast into the Minnesota 

River-Red River lowlands. Because of the lack of ground-water data within 

the reservation, this study did not attempt to address the delineation of 

aquifers identified within the reservation in other studies (Leap, 1972; 

Koch, 1975) . More detailed data and interpretation are needed to establish 

the definite boundaries and extent of aquifers in the reservation.

The depth from land surface to the first sand and gravel deposits 

thicker than 3 ft in the reservation is illustrated in figure 17. Large 

areas of sand and gravel deposits are at or near land surface, and probably 

are areas of water recharge to or water discharge from those deposits. This 

map was developed to generally indicate how deep a driller could expect to 

drill before encountering the first significant sand and gravel deposits. 

The map is not suitable for delineating the extent of aquifers. Such an 

effort will require additional data and numerous cross sections to determine 

elevations and possible continuity of sand and gravel deposits. Those 

analyses were beyond the scope of this study.

The thickness of sand and gravel deposits also is shown in figure 17. 

Surficial sand and gravel deposits in the Coteau range in thickness from less 

than 3 ft to 70 ft, and average 25 ft. Shallow sand and gravel deposits in 

the Minnesota River-Red River lowlands range in thickness from less than 

3 ft to 70 ft near the Minnesota-South Dakota border (fig. 17). These thicknesses of sand and gravel should provide some indication of the location of 

substantial quantities of water within those deposits, although in a few 

instances the first significant sand and gravel deposits penetrated were dry.

Multiple layers of sand and gravel deposits underlie the Coteau, but are 

particularly prevalent in the Minnesota River-Red River lowlands. Many of 

these layers in the lowlands of the reservation tend to be deep (90 to 250 ft 

below land surface) and may be 10 to 60 ft thick. Some deep sand and gravel 

deposits underlying the Minnesota River-Red River lowlands may directly overlie Cretaceous sedimentary rocks.

Ground-water within the reservation generally tends to flow west and 

east-northeast from a topographic divide located along the eastern edge of 

the Coteau. Water levels for various wells are shown in figure 18. In 

several areas, water may flow from areas where sand and gravel deposits are 

within 5 ft of the land surface, indicating possible areas of recharge. The 

available water-level data precluded the development of a ground-water flow 

regime.

32
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R.54W. R 53 W. R.52W. R.50W. R.49W, R.48W. R.47W.

Figure 17.--Depth below land surface and thickness of sand and gravel 

deposits in the Lake Traverse Indian Reservation.

33
* « . 3**s»i«*«H#»

."83 

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V 188.7 

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EXPLANATION

WELLS OR TEST HOLES-- 

Upper number indicates 

water level elevation in 

first water-bearing sands 

or gravel. Lower number 

is land surface elevation 

(1981-1982)

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R.54W. R.53W. R.52W. R.5IW. R.50W. R.49W. R 48W. R.47WFigure 18.--Water-table altitude in surficial sand or gravel in the 

Lake Traverse Indian Reservation.

34
Ground-Water Quality

In most instances, ground water is more mineralized than surface water. 

Reasons for this include longer contact time with water-soluble minerals, 

increased solubility of minerals because of higher temperature, and contact 

with clay layers with exchangeable ions.

Analyses of water samples from wells in the reservation indicate that 

significant increases in dissolved-solids concentrations generally occur as 

well depth increases (fig. 19). Median specific-conductance values range 

from about 1,400 /iS/cm (microsiemens per centimeter at 25 °C) in wells with 

depths ranging from 30 to 60 ft to 3,200 /iS/cm for wells with depths greater 

than 500 ft. Many of the wells deeper than 500 ft may be completed just 

above Cretaceous sedimentary rocks. Sodium, potassium, sulfate, chloride, 

fluoride, iron, manganese, and dissolved-solids concentrations also generally 

increase with well depth. Since censored data (data with less than a minimum 

value) were present (specifically iron, manganese, and nitrate) , a maximumlikelihood procedure was used to provide estimates of means and 25th, 50th, 

and 75th percentiles (Helsel and Gilliom, 1985). Concentrations of chloride 

in water samples from shallower wells only occasionally exceed South Dakota 

drinking-water standards (South Dakota Department of Water and Natural 

Resources, 1986), whereas concentrations of sulfate from wells frequently 

exceeded those standards (fig. 19). It is unknown whether the water quality 

in deeper wells is affected by recharge from the Dakota aquifer or if 

concentrations are larger because of the longer contact time between water 

and the deeper glacial-aquifer materials.

Although nitrate concentrations tend to be larger in water from the 

shallower wells, those samples infrequently exceeded the drinking-water 

standard for nitrate of 10 mg/L as nitrogen (fig. 19) (South Dakota 

Department of Water and Natural Resources, 1986). Infants may develop the 

disorder methemoglobinemia (blue-baby disease) when nitrate concentrations 

equal or exceed 10 mg/L as nitrogen. Although nitrate concentrations tend to 

decrease with well depth, water from the deeper wells contains nitrate in a 

concentration range similar to that in water from the shallower wells. It is 

possible that inadequate construction of the deeper wells could allow 

nitrate-enriched water from the shallow wells to flow down the outside of the 

well casing and into the deep sandstone aquifer (Dakota Sandstone).

Water in the shallow wells can become contaminated with large concentrations of nitrate through the placement of wells downgradient from livestock 

areas and septic-tank leach fields. It is unlikely that water with large 

nitrate concentrations would seep through the many layers of sand, gravel, 

and glacial till to reach the water in the deep wells; however, if the water 

could seep to deeper depths, the anoxic conditions of deep ground water would 

facilitate the denitrification of nitrate in the water by facultative microorganisms to produce reduced-nitrogen compounds including nitrogen gas and 

result in depletion of nitrate in the water.

In general, proportions of dominant cations changed little in water 

samples from wells with depths less than 500 ft below land surface. Calcium 

and magnesium proportions were stable at all well depths except the greatest 

depths. Calcium and magnesium consisted of at least 86 percent (on an equivalent basis) of the total cations at all well depths except the greatest 

depths.

Proportions of dominant anions were much more variable. Bicarbonate and 

sulfate were the predominant anions in most instances. However, in a few 

samples, chloride concentrations were a greater proportion of the anions than 

bicarbonate or sulfate.

35
SPECIFIC CONDUCTANCE TOTAL DISSOLVED SOUDS TOTAL ALKALINITY

15,000

10,000 15 13 46 28 17 34 11

1,000

1234567 

WELL-OEPTH CLASS

10,000

2 1,000

27 8 5 21 18 7 18

1234567 

WELL-OEPTH CLASS

1,000

I!-!<

dU

15 15 45 33 20 36 14

WELL-DEPTH CLASS

DISSOLVED CALCIUM

3,000

j 1,000

2,000

5 1,000

19 16 51 39 20 39 14

1234567 

WELL-DEPTH CLASS

DISSOLVED MAGNESIUM

19 16 51 39 20 39 14

WELL-DEPTH CLASS

EXPLANATION

45 -- NUMBER OF SAMPLES 

-- MAXIMUM

-- 75TH PERCENTILE

-- 50TH PERCENTILE (MEDIAN)

-- 25TH PERCENTILE

-- MINIMUM

 DETECTION LIMIT

 STATE SURFACE WATER QUALITY 

STANDARD FOR DOMESTIC 

WATER SUPPLY

WELL-DEPTH CLASS

1 Well depth less than 30 feet

2 Well depth 30 to 60 feet

3 Wel I depth 60 to 100 feet

4 Well depth 100 to 200 feet

5 Well depth 200 to 300 feet

6 Well depth 300 to 500 feet

7 Well depth greater than 500 feet

Figure 19.--Water quality of ground water by well depth in the 

Lake Traverse Indian Reservation.

36
CONCENTRATION, IN MICROGRAMS PER LITER CONCENTRATION, IN MILLIGRAMS PER LITER CO

CONCENTRATION, IN MICROGRAMS PER LITER CONCENTRATION, IN MILLIGRAMS PER LITER CO

CJ

CONCENTRATION, IN MILLIGRAMS PER LITER

CO
Water samples from wells less than about 180 ft deep had two different 

water types a calcium bicarbonate type and a calcium sulfate type and 

probably reflect water in the glacial aquifers or perhaps some intrusion of 

water from underlying Cretaceous sedimentary rocks through improperly constructed or corroded wells. Water from these wells is very hard (hardness 

greater than 180 mg/L as CaCO 3 ) and, although suitable for domestic and 

agricultural uses, many users prefer softer water.

Wells at a depth of greater than 500 ft below land surface generally are 

completed in the Cretaceous Dakota Sandstone and yield water that generally 

is too mineralized for most uses. The water generally is soft with predominant ions being sodium and sulfate (figs. 19 and 20). Two other water types 

are evident from wells in this grouping, calcium bicarbonate and calcium 

sulfate. It is likely that wells with those two water types are completed in 

deep glacial-outwash deposits with water quality similar to that in shallower 

glacial-outwash deposits. However, some intrusion of water from overlying 

glacial formations may produce local dilution of water from the Dakota 

Sandstone. Such intrusion results from improperly constructed deep wells 

that are cased through glacial sands and gravels and allow water to flow into 

the sandstone aquifer. However, no data are available to confirm that 

hypothesis.

Data pertaining to ground-water quality within the reservation are 

lacking for numerous areas. In addition, at least 50 percent of the waterquality samples for all aquifers could not be used to determine the dominant 

ions because of incomplete analyses. Additional water-quality samples could 

be collected at wells that now do not have complete analyses. It is possible 

that additional data on dominant ions could help delineate aquifer boundaries 

or determine if water is moving from one aquifer to another through 

improperly constructed wells or other avenues. Nitrate plus nitrite, 

dissolved-fluoride, dissolved-iron, and dissolved-manganese data are 

especially needed. Nitrate plus nitrite data are needed particularly from 

the glacial-outwash aquifers. Because these aquifers are close to land 

surface and are commonly used for private water supplies, they are 

particularly susceptible to contamination by nitrate plus nitrite in runoff 

from feedlots, septic tanks, and fertilizer storage areas.

NEEDED ADDITIONAL STUDIES

Although numerous data are available for surface and ground water within 

the reservation, and have been used in this investigation, key pieces of data 

are missing. This investigation has established that the quantity, timing, 

and storage of surface water within the reservation is not sufficient to meet 

large-scale beneficial uses. Lakes generally are too shallow and too 

affected by the vagaries of climate to be used as a large-scale water supply. 

Streamflow is not dependable for most of the year except during spring when 

the winter snowpack melts. Additional gaging stations could be used to 

monitor streams flowing from the reservation into Minnesota (Jorgenson River) 

and North Dakota (Shortfoot Creek).

Surface water generally is suitable for most uses. Because the streams 

and most lakes in the reservation are hydraulically connected to glacialoutwash aquifers, the water is suitable for domestic, industrial, and agricultural supplies. However, additional chloride, sulfate, nutrient, traceelement, fecal coliform and fecal streptococcus bacteria, and sedimenttransport data are needed for streams and lakes in the reservation. An indepth study of Bitter Lake and Lake Hillebrands could provide insight into 

hydrogeochemical processes in lakes within closed basins.

38
EXPLANATION 

Well depth less than 30 feet 

Well depth 30 to 60 feet 

Wel I depth 60 to 100 feet 

Well depth 100 to 200 feet 

Well depth 200 to 300 feet 

Well depth 300 to 500 feet 

Well depth greater than 500 feet

o o

CALCIUM " " CHLORIDE

PERCENT OF TOTAL MILLIEQUIVALENTS PER LITER

o 

o

Figure 20.--Trilinear plot of water chemistry by well depth for wells in 

and near the Lake Traverse Indian Reservation.

39
Because the quantity, timing, and storage capacity of surface water in 

the reservation preclude large-scale development, the ground-water resource 

becomes an important component in the reservation's use of water. Available 

data are not sufficient to describe with accuracy the direction of regional 

ground-water flow and the thickness of regional sand and gravel deposits in 

the reservation. Furthermore, additional water-level data are needed to 

further define areas of recharge and discharge; additional well logs are 

needed to further define elevation, thickness, areal extent of sand and 

gravel deposits, and delineation of aquifers. This additional data, plus 

tests to determine aquifer transmissivity and specific yield, will provide 

information that allows a more predictable and more efficient means of 

finding significant quantities of usable ground water. Additional data 

pertaining to the quality of ground water in the reservation are needed to 

ensure that available water meets drinking-water standards.

Although the data and interpretations in this report are sufficient to 

provide a general overview of ground water in the reservation, considerable 

additional data and interpretations are needed in order to efficiently 

develop the resource. Specifically:

1. Additional well-log data, which can be obtained either through 

surveys of existing wells or by drilling of observation wells, are 

needed in parts of the reservation to develop multiple lithologic 

sections of sand and gravel deposits for defining specific aquifers.

2. Measurement of water levels in as many wells as possible during a 

6-month period are needed to determine potentiometric surfaces of 

the aquifers and direction of ground-water flow on a local scale.

3. Tests are needed to determine aquifer transmissivity, specific 

yield, and storage coefficient.

SUMMARY

The Lake Traverse Indian Reservation in the northeast part of South 

Dakota occupies a triangular area within the Central Lowlands physiographic 

province. The topography is generally glacially derived and is characterized 

by two physiographic divisions the Coteau des Prairies (a prominent plateau) 

and the Minnesota River-Red River lowlands. Geologically, the area is underlaid by layers of glacial till and outwash, and alluvial deposits of sand and 

gravel. These deposits are underlaid by Cretaceous sedimentary rocks and 

Precambrian granite.

The glacial-outwash and alluvial deposits generally are layers of fine 

to coarse sand and gravel with poor to moderate sorting that are commonly 

interlayered with till. The thickness of sand and gravel deposits ranges 

from less than 3 ft to 70 ft; these deposits may extend from the land surface 

to depths greater than 230 ft below land surface. Cretaceous sedimentary 

rocks containing a sandstone aquifer underlie the reservation at depths 

greater than 500 ft below land surface.

Surface water within the reservation consists of intermittent streams 

and numerous lakes and wetlands. The reservation is located in parts of 

three major river basins: the Missouri River basin, represented by the Big 

Sioux and James River basins; the Souris-Red-Rainy River basin, represented 

by the Bois de Sioux River basin; and the Upper Mississippi River basin, 

represented by the Little Minnesota and Jorgenson River basins. The flow 

regimes of the Big Sioux, Bois de Sioux, and Little Minnesota Rivers have 

distinct seasonal trends. Most of the annual streamflow occurs from March

40
through June in response to the melting winter snow pack and to thunderstorms. Spring is the period of most dependable flow for the three rivers, 

but ground-water inflow in the basins of the Big Sioux and Little Minnesota 

Rivers provides a small but dependable flow during the fall. Periods of zero 

flow may occur during the winter and late summer.

Numerous lakes, ponds, and wetlands are located in the reservation, 

particularly within internally drained, noncontributing areas of the basins 

of the Big Sioux and James Rivers. These lakes store large quantities of 

water during wet periods (205,000 acre-ft in 1975); however, because of large 

surface areas, shallow depths, effects of evaporation, and lack of sustained 

ground-water inflow, the lakes cannot store dependable supplies of water for 

large-scale domestic or agricultural uses. Many of the lakes are hydraulically connected to glacial-outwash aquifers and lake levels tend to rise or 

fall with the water table.

Streamflow generally is suitable for most uses; dissolved-solids concentrations only occasionally exceed 1,000 mg/L in the Big Sioux, Bois de Sioux, 

and Little Minnesota Rivers. Other properties and constituents, such as pH, 

dissolved oxygen, and fecal coliform bacteria may exceed drinking-water 

standards and, in the case of bacteria, recreational standards. Nutrient 

concentrations may at times be large, indicating some enrichment from feedlots or septic tanks.

The lakes in the reservation may have dissolved-solids concentrations 

less than 500 mg/L (lakes in contact with glacial-outwash aquifers) or 

greater than 4,000 mg/L (lakes in contact with glacial till in closed 

basins). The water quality of many of the lakes indicates nutrient 

enrichment due to feedlot and other agricultural runoff; such enrichment 

accelerates eutrophication.

Ground water in the reservation generally is suitable for most uses; 

dissolved-solids concentrations commonly are less than 1,500 mg/L. The 

quality of water from the sand and gravel deposits generally is similar even 

to depths of 250 ft. However, nitrate may be a serious problem because 

concentrations approach the drinking-water standard of 10 mg/L as nitrogen. 

Water from the deep sandstone aquifer is too mineralized for domestic, 

irrigation, or industrial uses without treatment.

SELECTED REFERENCES

Flint, R.F., 1955, Pleistocene geology of eastern South Dakota: U.S. 

Geological Survey Professional Paper 262, 173 p.

Helsel, D.R., and Gilliom, R.J., 1985, Estimation of distributional 

parameters for censored trace-level water-quality data; II, Verification 

and applications: U.S. Geological Survey Open-File Report 85-86, 21 p.

Hodge, W.T., 1960, Climates of the States South Dakota: U.S. Department of 

Commerce, Weather Bureau, Climatography of the United States No. 60-39, 

16 p.

Hoffman, E.B., Freese, M.E., and Winter, D.R., 1986, Analyses of flood-flow 

frequency for selected gaging stations in South Dakota through September 

1985: U.S. Geological Survey Open-File Report 86-496, 137 p.

Koch, N.C., 1975, Geology and water resources of Marshall County, South 

Dakota Part I. Geology and water resources: South Dakota Geological 

Survey Bulletin 23, 76 p.

41
Leap/ D.I./ 1972/ Major aquifers and sand and gravel resources in Day County/ 

South Dakota: South Dakota Geological Survey Information Pamphlet 3, 

4 p.

Lindroth/ M. / 1976/ South Dakota water plan Resource inventory of the Big 

Sioux Coteau: South Dakota Department of Water and Natural Resources/ 

v. II-B/ sec. ll/ 135 p.

National Oceanic and Atmospheric Administration/ 1985, Climatography of the 

United States, No. 20, South Dakota: Asheville, N.C., National Climatic 

Data Center.

Roglin, E.N./ Goodman/ K.S./ and Conner/ T./ 1981, Test hole logs and well 

logs of Day County/ South Dakota: South Dakota Geological Survey OpenFile Report 3-C5/ 360 p.

Seaber, P.R./ Kapinos/ F.P., and Knapp/ G.L./ 1984/ State hydrologic unit 

maps: U.S. Geological Survey Open-File Report 84-708, 198 p.

South Dakota Department of Water and Natural Resources, 1975/ Development 

component of the South Dakota water plan Resource inventory of the Red 

River tributaries: v. II-B/ sec. 4/ 133 p.

 1986/ South Dakota water quality/ water years 1984-1985: Report to 

Congress of the United States pursuant to section 305(b) of the Federal 

Water Pollution Control Act (PL 92-500)/ 167 p.

State Lakes Preservation Committee, 1977, A plan for the classification, 

preservation/ and restoration of lakes in northeastern South Dakota: 

Prepared for the Governor and Legislature of South Dakota, 268 p.

U.S. Environmental Protection Agency, 1976, Quality criteria for water, 1976: 

Washington/ D.C./ U.S. Government Printing Office, 256 p.

 1986a/ Quality criteria for water/ 1986: Office of Water Regulations 

and Standards/ EPA 440/5-86-001/ unpaginated.

 1986b, Secondary maximum contaminant levels (section 143.3 of part 143, 

national secondary drinking-water regulations): U.S. Code of Federal 

Regulations/ Title 40/ Parts 100 to 149, revised as of July 1, 1986/ 

p. 587-590.

 1986c/ Maximum contaminant levels (subpart B of part 141, national 

interim primary drinking-water regulations): U.S. Code of Federal 

Regulations/ Title 40/ Parts 100 to 149, revised as of July 1, 1986/ 

p. 524-528.

* U. S. GOVERNMENT PRINTING OFFICE: 1989 -6S7-997/ 80

42