Sedimentation and 

Chemical Quality of Water 

in Salt Creek Basin 

Nebraska

By L. R. KISTER and J. C. MUNDORFF

CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1669-H

Prepared as part of a program of the 

Department of the Interior for development of the Missouri River basin

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1963
UNITED STATES DEPARTMENT OF THE INTERIOR 

STEWART L. UDALL, Secretary

GEOLOGICAL SURVEY 

Thomas B. Nolan, Director

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

Washington, D.C. 20402
CONTENTS

Page

Glossary _ _ _________________________________________________________ v

Abstract__________________________________________________________ HI

Introduction._ ______________________________________________________ 2

General features of the basin.._-_____-___-_____-_-_____-_-_-____-___-_ 2

Climate ________________________________________________________ 4

Vegetation and land use._________________________________________ 4

Geology._______________________________________________________ 5

Relief and drainage._____________________________________________ 10

Soils___________---_________-____--_-__-_________-___-_-_-_-__-- 11

Fluvial sediment___________________-___-___-_---_____---_-____-__-_- 13

Chemical quality of the water________--____-_-_-_-_-_-_-_--__-_-_-_-_- 24

Ground water-_-_____-_____-_-_-_____---_--____-_-_-_-_-_-_----- 24

Water from the Dakota group__________-___-_____---_-______ 28

Water from the sands and gravels of Pleistocene age _____________ 30

Water from the alluvium______________-___-_____--_--_-_-___- 30

Surface water._______________________-_-___-_-_____-_-_---_----_ 30

Water quality and use_ _ ____-_________-_-___-_-_______-__--_----_ 34

Domestic and public supplies______-_-______-__-__----_-_-_- 34

Industry-____-l___-_-_____________-_---_-_---_---_-_------- 38

Irrigation___ ___________-___-___-_-_-_-___-___-_-_---_-____-- 38

Summary ____ ____-_______-_________-_____-___---___-___---_-__------ 46

Selected bibliography________________________________________________ 47

ILLUSTRATIONS

FIGURE 1-2. Map showing: Page

1. Sampling sites in the Salt Creek basin.______________ H3

2. Bedrock geology of Salt Creek basin_______________ 6

3. Section showing relations among topography, parent materials, and soil types in Salt Creek basin.______________ 11

4-6. Stage hydrographs and concentration curves, Salt Creek at 

Lincoln:

4. May 30to June 4, 1951--_---_----_-----_-_.___-_- 15

5. June 16-20, 1954._______________________________ 15

6. July 2-3, 1954_______________-_-_________.________ 16

7-8. Photographs showing Salt Creek at Lincoln:

7. At discharge of 28,100 cfs, June 2, 1951____________ 18

8. At discharge of about 70 cfs____---__--_-____-_---_- 19

9. Graph showing relation of sediment discharge to water discharge, Salt Creek at Lincoln.-.-_________--__------_- 20

10. Flow-duration curve, Salt Creek at Lincoln, 1950-59_____ 22

in
IV CONTENTS

Page

FIGURE 11. Diagram showing percentage of sand, silt, and clay in suspended-sediment samples, Salt Creek at Lincoln_________ H23

12. Well-numbering system-________---_-_-_-_-_--__-_____- 25

13. Graph showing relation of chloride, dissolved solids, and type

of water from the Dakota group, Salt Creek basin_______ 29

14. Diagram showing concentrations of dissolved solids and 

chloride in surface water during periods of low discharge, 

Salt Creek basin___________________________________ 35

15. Graph showing relation of dissolved solids, discharge, and

water type, Salt Creek at Lincoln___________________ 37

16. Diagram showing classification of water for irrigation,_ _ ___ 44

TABLES

Page 

TABLE 1. Annual precipitation during 1950-58 at some locations in

Salt Creek baBin_____-___-____..------___---------- H4

2. Summary of rock formations younger than Permian age in

Salt Creek basin...._______-_________-_----_--_-______ 8

3. Monthly and annual summary of water and suspended-sediment discharge, Salt Creek at Lincoln__________________ 14

4. Measured suspended-sediment discharge, total sediment 

discharge, and hydraulic data for selected dates at Salt 

Creek at Lincoln______-_-__-___-----_------------_--- 23

5-7. Chemical analyses of:

5. Ground water, Salt Creek basin--..-__-_-_--_---_-___- 26

6. Surface water, Salt Creek basin__________-__--____- 31

7. Water from public supplies, Salt Creek basin________._ 40

8. Water-quality tolerances for industrial use_----_-________ 42
GLOSSARY

Equivalents per million (epm) is a unit for expressing the concentration of chemical constituents in terms of the interreacting values 

of the electrically charged particles, or ions, in solution. One 

equivalent per million of a positively charged ion will react with 

one equivalent per million of a negatively charged ion. Parts per 

million are converted to equivalents per million by multiplying by 

the reciprocal of the combining weight of the ion.

Cations Factor

Calcium (Ca+<0 _ __________ 0. 04990

Magnesium (Mg+2 ) __________ . 08226

Sodium (Na+i)_-__-____ _ .04350

Potassium (K+0 ____________ . 02557

Anions Factor

Carbonate (CO3-2 ) ------- 0.03333

Bicarbonate (RCCV1 )____-_ .01639

Sulfate (SO4-2 )_-_---------- .02082

Chloride (Cl-1 )----------- .02821

Fluoride (F-»)_____._.... .05264

Nitrate (NOs- 1 )------------- .01613

Fluvial sediment is sediment that is transported by, suspended in, 

or deposited from water.

Parts per million (ppm) is a unit for expressing the concentration 

of chemical constituents by weight, usually as grams of constituents 

per million grams of solution. Parts per million for suspended 

sediment is computed as one million times the ratio of the weight of 

sediment to the weight of the mixture of water and sediment.

Particle-size classification is the classification recommended by the 

American Geophysical Union Subcommittee on sediment terminology (Lane and others, 1947, p. 937). According to this classification, a particle having a diameter between 0.0002 and 0.004 mm 

is clay, a particle having a diameter between 0.004 and 0.062 mm 

is silt, and a particle having a diameter between 0.062 and 2.0 mm 

is sand.

Percent sodium is the ratio, expressed in percentage, of sodium to 

the sum of the positively charged ions (calcium, magnesium, sodium, and potassium) all ions given in equivalents per million.

Specific conductance is a measure of the ability of a water to conduct 

an electrical current and is expressed in micromhos per centimeter at 

25°C. Because the specific conductance is related to the number 

and specific chemical types of ions in solution, it can be used for
VI GLOSSARY

approximating the salinity of the water. The following general 

relations are applicable:

Specific conductance X (0.65 ± 0.05) =ppm dissolved solids; 

Specific conductance_ total epm 

100 = 2'

Suspended sediment is the sediment that at any given time is maintained in suspension by the upward components of turbulent currents or that exists in suspension as a colloid.

Water discharge of a stream is the flow of the stream and includes 

the sediment and dissolved solids that are contained in the water. 

Water type, in this report, indicates the predominant cation and 

anion present.
CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

SEDIMENTATION AND CHEMICAL QUALITY OF WATER 

IN SALT CREEK BASIN, NEBRASKA

By L. R. KISTER and J. C. MTJNDORFF

ABSTRACT

Salt Creek basin occupies about 1,655 square miles of the dissected till plains 

of eastern Nebraska. Surficial deposits, in the basin range from alluvial and 

eolian deposits of Recent age to limestones and shales of Pennsylvanian age. 

Deposits of Pleistocene age, mainly loess and glacial till, mantle nearly the entire 

basin; scattered bedrock outcrops are mainly along the major stream valleys. 

Sedimentary rocks of the Dakota group of Early Cretaceous age immediately 

underlie deposits of Pleistocene age in most of the basin. In about 40 square 

miles in the western part of the basin, the Greenhorn limestone and (or) 

Graneros shale of Late Cretaceous age immediately underlie deposits of Pleistocene age. Limestones and shales of Permian age compose the uppermost bedrock in the southeastern part of the basin. Limestones and shales of 

Pennsylvanian age compose the uppermost bedrock in and bordering Salt Creek 

valley from Lincoln to the mouth of Salt Creek.

The climate of the basin is continental and subhumid. Average annual precipitation at Lincoln is 25.73 inches; during 1921-55 annual precipitation ranged 

from 14.09 inches in 1936 to 40.1 inches in 1951.

Most of the total annual suspended-sediment discharge of Salt Creek occurs on 

a few days of each year. In most years, 75 percent or more of the total annual 

discharge occurs on 15 or less days.

Flow-duration data for 1950-59 and sediment-discharge data for 1951-54 indicated that the total suspended-sediment discharge at Lincoln for 1950-59 was 

about 18.7 million tons. A layer of soil 1 foot thick and about 13 square miles 

in area would be required to yield this estimated discharge.

Computations of total sediment discharge indicated that bedload discharge is 

a minor part of the total sediment discharge over wide ranges of water and 

sediment discharges. The suspended sediment transported by Salt Creek is 

predominantly clay and silt.

Water from most wells in the Dakota group contained high concentrations of 

dissolved solids and was of the sodium chloride type. The water from some of 

the wells, however, contained less than 500 ppm (parts per million) of dissolved 

solids and was of the calcium bicarbonate type; such water generally overlies 

the water containing higher concentrations of dissolved solids.

Water from the sands and gravels of Pleistocene age in the southern half of the 

basin contained generally less than 1,000 ppm of dissolved solids, and water in

HI
H2 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

the northern half contained generally less than 500 ppm. Locally in the southern half of the basin, water from the Dakota probably infiltrates: the sands and 

gravels of Pleistocene age. Except where the water from the Dakota affects 

the water in the sands and gravels of Pleistocene age, the water is of the calcium bicarbonate type.

Not much information is available on the quality of the water in the alluvium; 

however, the water probably is of the calcium bicarbonate type and has less 

than 1,000 ppm of dissolved solids, except where water of the sodium chloride 

type has infiltrated the alluvium.

During low discharge the water in the upstream parts of Salt Creek and its 

tributaries is similar in chemical quality to the water from sands and gravels 

of Pleistocene age, and the water in the vicinity of Lincoln is similar in chemical 

quality to the water from the Dakota group.

Nearly all the water used in the Salt Creek basin for domestic, public, and 

industrial supplies is produced from wells; surface water of adequate quantity 

and quality is not available. Water from most public supplies contained less 

than 500 ppm of dissolved solids but was very hard. Iron and manganese in 

many of the supplies exceeded recommended maximum concentrations. The 

water from the Dakota group is either unsatisfactory for irrigation or is 

insufficient for large-scale irrigation. Most of the water from the deposits 

of Pleistocene age and from the alluvium can be used for irrigation if drainage 

is adequate and if plants having good salt tolerance are grown.

INTRODUCTION

The U.S. Geological Survey began studies of water quality in the 

Salt Creek drainage basin in 1950 as a part of the program of the 

Department of the Interior for the development of the Missouri River 

basin. Chemical-quality studies have been made of the water from 

Salt Creek and its tributaries and from three types of water-bearing 

deposits the Dakota group of Early Cretaceous age, the sands and 

gravels of Pleistocene age, and the alluvium of Recent age. Fluvialsediment studies have been made only at one site, Salt Creek at Lincoln. 

The interpretive results of these studies are presented in this report.

These studies were made under the supervision of P. C. Benedict, 

regional engineer, who was succeeded by D. M. Culbertson, district 

engineer. The geology section of the report was prepared from information furnished by E. C. Reed, Director of the Conservation and 

Survey Division, University of Nebraska.

GENERAL FEATURES OF THE BASIN

Salt Creek basin, a part of the dissected till plains of eastern Nebraska, is about 1,655 square miles in area and comprises parts of six 

counties. (See fig. 1.) Of the total area, about 75 percent is cultivated, about 20 percent is pasture, and about 5 percent is urban and 

wasteland. The estimated population of the basin is about 150,000, 

of which about 80 percent is urban. Although the population is pre-
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H3

R. 6 E. R.7E.

R. 5 E

R. 9 E.

R. 10 E.

INDEX MAP

10123456 MILES

FIGURE 1. Map showing sampling sites in the Salt Creek basin, Nebraska. 

690-193 O 63 2
H4 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

dominantly urban, the economy of the basin is based mainly on agriculture ; other significant economic enterprises include manufacturing 

industries, transportation industries, and military installations.

CLIMATE

The climate of Salt Creek basin is continental and subhumid. An 

annual temperature range of 110°F and winter temperatures of 0° 

to -10°F and summer temperatures of 100° to 105°F are common. 

Weather Bureau records show that the minimum was 29°F and 

the maximum was 115 °F during the period 1900 to 1960.

Average annual precipitation at Lincoln for 1921-55 was 25.73 

inches (reported by the U.S. Weather Bureau) and for 1950-58 was 

nbout 28.7 inches (computed from U.S. Weather Bureau records); 

the minimum was 14.09 inches in 1936, and the maximum was 40.1 

inches in 1951. Although U.S. Weather Bureau records for 1956 

show that the total precipitation at Lincoln was about 23.8 inches, 

which is near normal, the total at Valparaiso, in the northern part 

of Salt Creek basin, was only 12.7 inches.

Generally, about 55 percent of the total precipitation occurs between 

May and August, and about 75 percent occurs between April and 

September. Annual snowfall averages about 24 inches. The variability of precipitation from year to year and from place to place in 

the basin is apparent from data shown in table 1.

TABLE 1. Annual precipitation, in inches, during 1950-58 at some locations in 

Salt Creek basin, Nebraska

[From U.S. Weather Bureau records]

Location

Lincoln _______ .......

Raymond.... ___ ..,. ... ..

Valparaiso ___ .. .....

1950

24.8

18.0

20.6

26.0

32.2

1951

40.1

41.2

40.0

41.4

1952

32.0

28.6

26.8

27.9

29.6

30.7

1953

21.2

17.5

19.4

19.9

22.4

20.2

1954

30.6

24.7

26.8

22.2

28.1

32.1

1955

U7

21.0

17.6

19.7

18.3

14.5

1956

23.8

18.5

20.4

12.7

14.3

27.1

1957

34.6

36.0

35.6

30.6

34.2

31.4

1958

33.9

36.7

32.6

27.8

21.2

29.1

Partly estimated.

VEGETATION AND LAND USE

In preagricultural time, the vegetation consisted mainly of tall 

grass, such as little bluestem, big bluestem, needlegrass, and side-oats 

grama; trees were restricted to stream valleys. Before about 1870 

only a minor part of the land in Salt Creek basin was cultivated; 

between about 1870 and 1900 a major part was placed in cultivation. 

Since 1900 changes in cultivated acreage have been relatively minor. 

The principal crops include corn, sorghums, wheat and other small 

grains, and legumes.
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H5

During recent years considerable progress has been made in instituting land-use practices to'reduce erosion and surface runoff. Some 

marginal land has been retired from production of cultivated 

crops and has been seeded to grass. Contour farming and terrace 

farming are common on much of the cultivated land.

GEOLOGY

Deposits exposed at the surface in the Salt Creek basin range from 

alluvial and eolian deposits of Kecent age to limestones and shales 

of Pennsylvanian age. Unconsolidated deposits of Pleistocene age 

mantle nearly the entire basin; the scattered outcrops of rocks of 

Pennsylvanian, Permian, or Cretaceous age are limited to steep valleyside slopes, mainly along the major streams. Only the rocks of 

Pennsylvanian age or younger significantly affect the ground-water 

hydrology, water quality, and runoff in the basin. Rocks older than 

Pennsylvanian age therefore, are not discussed in this report.

Kocks of Pennsylvanian and Permian age consist mainly of interbedded limestones and shales and, in general, have low permeability 

except where highly weathered or fractured. Limestones and shales 

of Permian age compose the uppermost bedrock (fig. 2) in the southeastern part of the basin but crop out only along the valley of Salt 

Creek. Limestones and shales of Pennsylvanian age compose the 

uppermost bedrock in and bordering Salt Creek valley from Lincoln 

to the mouth of Salt Creek but crop out only in a few places near 

Ashland.

The sandstones and shales of the Dakota group immediately underlie glacial till in most of the basin. (See table 2.) The rocks of the 

Dakota group differ widely in permeability; the sandstones have high 

permeability, and the shales have low permeability. Kocks of the 

Dakota group crop out at many places along the valleys, mostly in 

Lancaster County. The Dakota group has a maximum thickness of 

about 400 feet in the western part of the basin and thins progressively 

eastward.

In about 40 square miles in the western part of the basin, the 

Dakota group is overlain by rocks of Late Cretaceous age, the Graneros shale and the Greenhorn limestone; the Graneros shale is 

overlain by the Greenhorn limestone. The Graneros shale is as much 

as 70 feet thick, and the Greenhorn limestone is as much as 30 feet 

thick. The Greenhorn crops out about 3 miles north-northeast of 

Garland in a small area along the valley of Middle Oak Creek.

Deposits of Pleistocene age are at or near the surface in most of 

the basin and differ greatly in thickness, composition, and lateral 

extent. The surface material and topography of the basin have re-
H6 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

PLATTE

ASS

^^

EXPLANATION

Rocks of 

Dakota group

Rocks of 

Permian age

Line of section shown 

on figure 3

FIGURE 2. Bedrock geology of Salt Creek basin (from Reed, 1951).

(/)

WA¥/M

Rocks of 

Pennsylvanian 

age

PENNSYLVANI CARBONIFERO
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H7

suited almost entirely from deposition and erosion since the beginning 

of the Pleistocene epoch.

As the earliest Pleistocene continental glacier (Nebraskan) advanced from the northeast, the sands and gravels of the David City 

formation were deposited in the lower parts of the valleys. The eastward-flowing streams were dammed or were deflected southward by 

the advancing ice sheet, which overrode the channel fills of sand and 

gravel. When the glacier receded northward, the Nebraskan drift, a 

poorly sorted boulder-clay deposit from the melting ice, remained as 

a mantle over the surface. The streams that were formed in this 

surface by melt water from the receding glacier deposited the sands, 

gravels, silts, and clays of the Aftonian formation (E. C. Reed, written communication).

A similar sequence of events occurred as the second continental glacier (Kansan) advanced over and receded from the area. Sands and 

gravels of early Kansan age, Kansan drift, sands and gravels of the 

Grand Island formation, and the silts and clays of the Sappa formation remain as evidence of the advance and recession of the Kansan 

glacier. At the end of Kansan time the present valleys of the basin 

began to be formed. The Grand Island formation is closely associated 

with present major valleys, because no glaciers advanced over the 

basin after Kansan time. However, variation in the climate during 

the advance and recession of the Illinoian, early Wisconsin, and late 

Wisconsin glaciers, which were north and east of the basin, caused 

three principal cycles of deposition that were separated by periods of 

weathering and soil development. During Illinoian time, the Crete 

formation and the Loveland loess were deposited; during early Wisconsin time, the Todd Valley formation and the Peorian loess were 

deposited; during late Wisconsin time, localized alluvium and the 

Bignell loess were deposited. During interglacial periods the Sangamon or Loveland soil developed on the Loveland loess, and the 

Brady soil developed on the Peorian loess.

The alternate degradation and aggradation of the valleys in postKansan time resulted in at least four terrace levels. Some of the terrace levels are indistinct because successive cuts removed parts of 

the previous terrace levels, which were then replaced by younger terrace fills. Some of the highest levels are indistinct because of valleyside erosion.

Valley alluvium of Recent age was deposited along the streams 

during floods. The presence of natural levees 2 to 3 feet higher than 

the adjoining bottom land is evidence of repeated flooding in the past. 

The natural levees and the flood plains indicate that floods have been 

common in Salt Creek valley.

Cretaceous

Nebraskan

Aftonian formation

Nebraskan drift

David City formation

Greenhorn limestone

Graneros shale

Dakota group

Light-gray silts and clays locally grading to fine sand; in many places leached at top; comparatively 

extensive in the subsurface; crops out along the valley sides at low levels in the southern part of 

the basin and at progressively higher levels northward; 0 to 60 ft thick.

Dark-gray boulder clay that contains fewer and smaller boulders and pebbles than are in the Kansan 

drift; upper surface weathered and leached and some gumbotil has formed locally; locally crops 

out in the northern part of the basin but is largely limited to the subsurface; 0 to 50 ft thick.

Sand and gravel that occur as channel fills; do not crop out at the surface but are known to interflnger with Kansan drift in the subsurface; 0 to 60 ft thick.

Light-gray to white dense to chalky limestone; contains numerous clam shells; crops out northeast 

of the town of Garland and is limited to the northwestern part of the basin; 0 to 30 ft thick.

Dark -gray shale, chalky in upper part, sandy in lower part; limited to the subsurface of a small area 

in the northwestern part of the basin; 0 to 70 ft thick.

Sandstones and shales; upper 160 ft is generally sandstone but may grade laterally to gray or varicolored clay shales; middle 60 ft is red and varicolored clay shales; lower 100 ft is mostly sandstone.

!

<£> w
H10 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

Much of the terrace and upland surface of the basin is mantled 

with Peorian loess or Bignell loess except in western Lancaster County 

and southwestern Saunders County, where these loesses are extremely 

thin or absent. In such areas, Kansan drift is at or near the surface. 

The thickness of Peorian loess and Bignell loess ranges from 0 feet 

in some areas to about 40 feet in the northern part of the basin.

BELIEF AND DRAINAGE

The present surface of Salt Creek basin conforms, in major aspects, 

to the Kansan drift surface. Prior to deposition of Loveland loess, 

the Kansan drift surface was subjected to erosion and dissection, which 

produced a rolling to hilly topography. The irregularities of the 

dissected drift surface were somewhat subdued by subsequent loess 

deposition. Either most of the Loveland loess was removed by erosion prior to deposition of the Peorian loess or the Loveland loess 

deposited in this area was thin. In many areas erosion has removed 

both the Loveland and Peorian loess and has exposed the underlying 

glacial drift.

The greatest relief in Salt Creek basin is in northwestern Lancaster 

County, in southeastern Butler County, in the headwaters of Wahoo 

Creek, and in the "Bohemian Alps" in east-central Seward County. 

Local relief generally ranges from 100 to 200 feet in these areas. 

Altitudes range from about 1,040 feet at the mouth of Salt Creek to 

about 1,620 feet in the extreme northwestern part of"the basin.

The most extensive terraces are mainly along Salt Creek in the 

vicinity of Lincoln and Waverly and in Todd Valley in the northeastern part of the basin. These terraces generally have a loess or silt 

mantle that is underlain by a variable thickness of sand and gravel.

The basin is generally well drained, and drainage problems are 

minor. The only poorly drained areas of significance are in the alluvium bordering some of the large streams; in some of these areas the 

high concentration of salts in the soil retards or prohibits plant 

growth. Salt efflorescence may occur during dry periods. The upland 

areas are well drained except for scattered small" depressions.

The stream system of Salt Creek basin has a dendritic pattern, which 

is, however, not ideally formed. The effect of bedrock in the control 

of the detailed drainage pattern is very minor. The downstream twothirds of Salt Creek and long reaches of some of the major tributaries, 

however, are in bedrock-defended valleys; the channels are at a lower 

elevation than is the bedrock along the valley sides.

Throughout most of the length of Salt Creek and in the downstream reaches of the major tributaries, the natural channels are 

meandering. The sinuosity indexes of these channels, computed as
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. Hll

the ratio of channel length to valley length, range from about 1.5 to 

about 2.0. Leopold and Wolman (1957) arbitrarily classified streams 

having sinuosity indexes greater than 1.5 as meandering "streams. 

Between Lincoln and Ashland, the Salt Creek channel has been 

straightened and enlarged to increase its capacity. The channel had 

a sinuosity index of about 1.9 before straightening and about 1.2 after 

straightening. The gradient of Salt Creek was increased from about 

1.7 feet per mile before straightening to about 2.7 feet per mile after 

straightening.

SOILS

Salt Creek basin is usually described as being in the Prairie soil 

region of the United States, although most of the basin occupies a 

transitional zone between the Prairie and Chernozem soil zones. All 

the soils have developed under the influence of tall-grass vegetation 

except those soils occupying part of the bottom lands and part of the 

most steeply sloping uplands.

Each soil type occupies a rather characteristic topographic position. 

(See fig. 3.) Where loessial and glacial soils are associated within

WE!

i 3

>T

HHI 3 2 5 6 4 3 1 4 1 5 3 2 3 2

EAST

«IM 4 3 5 5

EXPLANATION

PARENT MATERIALS

ALLUVIUM

PEORIAN LOESS

TOOD VALLEY FORMATION

LOVELANO LOESS

CRETE FORMATION

SAPPA FORMATION

GRAND ISLAND FORMATION 

GLACIAL OUTWASH SAND 

KANSAN DRIFT 

AFTONIAN FORMATION

l;ft> X :.V-| NEBRASKAN DRIFT

PARENT MATERIAL AND SUBSURFACE 

GEOLOGY INFERRED FROM BEES LEY 

AND OTHERS (1948); CONOR A AND 

REED (1943, 1950)

SOI LS

1. CARRINGTON LOAM AND SILTY CLAY LOAM

2. WAUKESHA SILTY CLAY LOAM

3. WABASH SILT LOAM

4. SHARPSBURG SILTY CLAY LOAM

5. CRETE SILTY CLAY LOAM

6. DICKINSON SANDY LOAM

FIGURE 3. Relations among topography, parent materials, and soil types in Salt Creek 

basin. Line of section is from sec. 3, T. 10 N., R. 5 E., to sec. 1, T. 10 N., R. 7 E. Vertical 

scale is exaggerated.

690-193 O 63-
H12 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

relatively small areas, the loessial soils are commonly developed along 

the upper slopes and ridge tops, and the glacial soils are generally 

some distance downslope. In most of the eastern and northern parts 

of the basin, however, soils are developed on a nearly unbroken mantle 

of loess.

Soils of the Butler, Crete, Sharpsburg, and Knox series are developed on the loessial uplands of the basin. Soils of the Carrington, 

Burchard, Pawnee, and Steinauer series are developed on the glacial 

uplands. The Waukesha and Rokeby series occupy terrace positions. 

The Wabash, Lamoure, Bremer, Judson, and Sarpy series are developed on alluvial and colluvial materials of the bottom lands. The 

soils of the basin are differentiated on the basis of texture of the 

different horizons in the profile, depth of solum, character of the parent 

material, and topographic position. Detailed soils maps are available only for part of the basin, and accurate computations cannot 

be made for the percentage of the basin occupied by different soils. 

On the basis of a soil survey of Lancaster County (Beesley and others, 

1948), geologic information, and reconnaissance throughout the basin, 

the following estimates were made: Loessial soils, predominantly of 

the Sharpsburg and the Crete series, about 60 percent of the basin; 

glacial till soils, predominantly of the Carrington * and Burchard 

series, about 20 percent; and terrace and bottom-land soils, predominantly of the Waukesha and the Wabash series, about 20 percent. Musgrave (1957) classified some of the major soils of the United 

States into "hydrologic soil groups." The classification is based on 

the premise that soils with similar profiles will respond in a similar 

manner under a long storm of appreciable intensity. Musgrave includes the Carrington, Sharpsburg, and Waukesha soils in the group 

described as "mostly sandy soils * * * and loess * * * [that have] 

above-average infiltration after thorough wetting"; the Burchard, 

Shelby, Butler, Crete, Steinauer, and Bremer soils in the group described as "shallow soils and soils containing considerable clay and 

colloid * * * [that have] below-average infiltration after presaturation"; and the Pawnee and Wabash soils in the group described 

as "mostly clays of high swelling percent [highest runoff potential]." 

Comparisons between the different soils are made with the assumption that the soils have minimum cover, that maximum swelling 

has taken place, and that the applied rainfall exceeds potential infiltration (Musgrave, 1957). The classification of hydrologic soil 

groups can be used to estimate runoff from a given area and to estimate 

roughly the erosion and sediment yield from a given area.

1 In November 1959, the term Carrington soil series was discontinued ; the present (1961) 

equivalent of the Carrington in eastern Nebraska is generally the Shelby series (A. R. 

Aandahl, oral communication).
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H13 

FLUVIAL SEDIMENT

Investigation of fluvial sediment in Salt Creek at Lincoln was begun 

in May 1950. From May 1950 to March 1951 and from October 1951 

to March 1952, suspended-sediment samples were obtained infrequently, usually during high stages. From March to September 1951 

and from March 1952 to September 1954, samples were obtained 

daily or at such frequency necessary to compute the daily suspendedsediment discharge. Analyses for most of the samples have been published by the U.S. Geological Survey in the annual series of watersupply papers entitled, "Quality of Surface Waters of the United 

States." The sampling location is shown on figure 1.

Suspended-sediment discharge is computed as the product of the 

measured suspended-sediment concentration, the total water discharge, 

and a constant for converting the units to a weight per unit time, 

generally tons per day. Suspended-sediment concentrations for computing sediment discharges were determined from depth-integrated 

samples collected with standard samplers. The suspended-sediment 

concentration, in parts per million by weight, was determined in the 

laboratory. Particle-size distribution of the sediment was determined 

by the sieve method or by methods based on the fall velocity of the 

sediment particles.

Table 3 is a monthly and annual summary of suspended-sediment 

data for Salt Creek at Lincoln for March to September 1951 and for 

March 1952 to September 1954. Most of the total annual suspendedsediment discharge of Salt Creek occurs on a few days of each year. 

During March to September 1951 the suspended-sediment discharge 

for 15 days was about 78 percent of the total discharge for the period. 

During March to September 1952 the suspended-sediment discharge 

for 12 days accounted for about 75 percent of the total for the period. 

Tn 1953 the suspended-sediment discharge for 5 days accounted for 

about 75 percent of the total annual discharge. In 1954 the discharge 

for 12 days accounted for about 87 percent of the total annual discharge. The combined suspended-sediment discharge for 5 days in 

June 1951 was about the same as the combined suspended-sediment 

discharge for the entire 1952,1953, and 1954 water years.

During the period March 1951 to September 1954, the measured suspended-sediment concentrations ranged widely (from 9 to 69,100 

ppm). The daily mean concentrations did not range as widely (from 

10 to 34,000 ppm). The daily mean concentrations for the period 

March 1951 to September 1954, if regarded as representative of longterm conditions, can be used to estimate the percentage of tune that 

specific daily mean concentrations would be exceeded. The data for 

this period indicate that a daily mean suspended-sediment concentra-
H14 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

TABLE S. Monthly end, annual summary of water and suspended-sediment 

discharge, Salt Creek at Lincoln, Nebr.

Month

1951 

Mar. 16-31.. ..........

April................................

June ___________________

July.......... .......................

August ____________ __ _ .

September ________________

Total, Mar. 16 to Sept. 30..

1962 

Mar. 16-31.................... ..

April. .... __ . ____________

June ______________ .

July........-................ .,.....

August ____________ .

September. _____ _____ .

Total, Mar. 16 to Sept. 30...

1963

March _________________ . .

April......................................

May. ____________ .. ..

June _____________ __

July.......................................

Total, water year 1952-53 ...........

1964

April......................................

June __________ ....................

July.................. __.....__...__._...._

Water 

discharge 

(cfs-days)

3,313

9,804 

14,341 

91,834 

7,687 

12,308 

8,098

147, 385

10,863 

19,129 

9,528 

22,948 

16,380 

5,921 

2,171

86,940

1,755 

2,085 

2,302

2,683 

4,152 

3,394 

3,229 

4,724 

2,299 

2,509 

1,950 

1,410

32, 492

1,099 

1,703 

1,700

1,271 

1,885 

1,658 

1,916 

6,674 

17, 550 

4,221 

17,604 

1,673

58,954

Suspended sediment

Load (tons)

59,358 

277, 154 

555,074 

4, 326, 702 

45,233 

312,440 

59, 817

5, 635, 778

410, 310 

469, 145 

102, 462 

838,405 

332, 110 

88,468 

1,274

2,242,174

197 

664 

490

1,160 

5,029 

1,156 

4,041 

22,208 

7,158 

48,774 

568 

585

92,030

160 

1,138 

605

155 

751 

306 

5,720 

119,455 

420,256 

115, 030 

191, 265 

215

855,056

Daily load (tons)

Maximum

136,000 

178,000 

857, 000 

12,000 

79,600 

20,000

199,000 

120,000 

35,200 

662,000 

184,000 

27,000 

796

9 

368

1500

103 

1,750 

10,600 

6,060 

44,900 

1200 

383

44 

800 

1200

1260 160 

4,770 

60,900 

263,000 

103,000 

60,800

Minimum

34 

118 

562 

11 

15 

3

99 

50 

10 

10 

9 

6

4

10 

9 

11 

1

12

U5

Maximum 

daily concentration 

(ppm)

21,600 

22,500 

34,000 

11,000 

22,000 

4,850

24,500 

10, 500 

20,500 

13,500 

18,000 

1,170

58 

846

350 

3,080 

6,300 

5,670 

14,400

160 

1,000

5,800 

10,900 

13,400 

12,700 

6,380

i Estimated.

tion of 50 ppm would be exceeded about 70 percent of the time; a concentration of 100 ppm, about 43 percent of the time; a concentration of 

500 ppm, about 23 percent of the time; a concentration of 1,000 ppm, 

about 17 percent of the time; a concentration of 5,000 ppm, about 6
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. HIS

percent of the time; and a concentration of 15,000 ppm, only about 1 

percent of the time.

HCOICENTRATION

\

40,000 "-

30,000 <-> u

FIGURE) 4. Stage hydrograph and concentration curve, Salt Creek at Lincoln, May 30 to

June 4, 1951.

GAGE HEIGHT

18

I

24,000

16,000 <* r)

2

Q?

JUNE

FIGDRB 5. Stage hydrograph and concentration curve, Salt Creek at Lincoln, June 16-20,

1954.
HI6 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

10

4 *= 

\

\

\

GAGE HEIGHT

^^-CONCENTRATION

X \

\

\

3 6 

JULY 2

70,000

60,000

LU 

50,000 Qcr 

<

CL

z 

40,000 

z"

o

. I- 

< 

tri30,000 Z

z

20,000 LU

10,000

3 6

JULY 3

FIGURE 6. Stage hydrograph and concentration curve, Salt Creek at Lincoln, July 2-3,

1954.
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H17

Hydrographs and concentration curves for selected periods of major 

flow of Salt Creek at Lincoln are shown in figures 4 to 6. During 

the flood of May 31 to June 4, 1951 (fig. 4), about 1,800,000 tons of 

suspended sediment was discharged; in contrast, during the entire 

1953 water year only 92,000 tons of suspended sediment was discharged. Figure 7 shows Salt Creek at Lincoln on June 2, 1951, 

at a discharge of 28,100 cfs, and figure 8 shows Salt Creek at a discharge of about 70 cfs.

The rapid rise at Lincoln on July 2, 1954 (fig. 6), was caused by 

heavy rain in the vicinity of Valparaiso, about 28 channel miles upstream, on the evening of July 1. Suspended-sediment samples were 

obtained immediately before the arrival of the flood wave and at frequent intervals during and after the passing of the flood wave. The 

suspended-sediment concentration increased from 75 ppm about 1 

minute before the flood wave arrived to 69,100 ppm at a discharge of 

1,200 cfs (cubic feet per second) about 10 minutes after the arrival 

of the flood wave. The suspended-sediment concentration then decreased gradually, although the maximum water discharge of 4,160 

cfs was not reached until about 6 hours after the maximum concentration occurred.

Possible reasons for the maximum concentration to precede the 

maximum water discharge are (1) the early runoff carries the most 

easily eroded weathered material from the drainage area, and (2) 

the sediment deposited in the channel during low-flow periods is eroded 

and placed in suspension by the initial flood wave as it moves downstream.

Runoff and sediment yield from any given area are controlled by 

many variables, such as geology, soil characteristics, slope, land use, 

type and density of channels, amount and intensity of precipitation, 

and flood- and erosion-control structures. The suspended sediment 

discharged by Salt Creek at Lincoln is composed of material derived 

from the western half of Salt Creek basin; for any given rise in stage, 

the exact part of the ba,sin from which the transported sediment was 

derived is rarely known. The sediment discharge at Lincoln, therefore, cannot be correlated with any single one of these variables or with 

any combination of the variables.

The relation of water discharge to sediment discharge at Salt Creek 

at Lincoln is fairly well defined. The curve in figure 9, based on both
HIS CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

FIGCEB 7. Salt Creek at Lincoln, June 2, 1951, at discharge of 28,100 cfs. A, Stage 

recorder (downstream side of bridge) ; B, Sampling installation (upstream side of 

bridge).
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H19

B

FIGURE 8. Salt Creek at Lincoln, at discharge of about 7O cfs. A, Stage recorder (downstream side of bridge) ; B, Sampling installation (upstream side of bridge).

690-193
H20 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

1.000,0001 

100,000

10 100 1000 10,000 50,000 

WATER DISCHARGE, IN CUBIC FEET PER SECOND

FIGURE 9. Relation of sediment discharge to water discharge, Salt Creek at Lincoln.
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H21

instantaneous discharge and on daily mean discharge, indicates that, 

on the average, sediment discharge increases as water discharge increases. An appreciable range in sediment discharge, however, can 

be expected at any given water discharge. For example, on Salt 

Creek the suspended-sediment concentration at a given water discharge 

is generally considerably higher on the rising stage than on the receding stage; therefore, the sediment discharge at a given water discharge 

may be considerably greater on the rising stage than on the falling 

stage. Nevertheless, the curve indicates the sediment discharge that, 

on the average, can be expected at any given water discharge.

The relation of sediment discharge to water discharge can be used 

in conjunction with a flow-duration curve or with streamflow data to 

estimate the probable suspended-sediment discharge during periods 

before and after sediment data are obtained on a stream. Figure 10 

is a flow-duration curve based on streamflow data obtained on Salt 

Creek at Lincoln during the period 1950-59. The total suspendedsediment discharge of Salt Creek at Lincoln for this period, computed 

from figures 9 and 10, was about 18.7 million tons and, computed from 

figure 9 and daily streamflow data, about 18.6 million tons.

If a specific weight of 100 pounds per cubic foot is assumed for the 

soil in place, a layer of soil about 1 foot thick and slightly more than 

1 square mile in area would yield about the same amount of sediment 

as that transported by Salt Creek at Lincoln in 1952. For the period 

1950-59, a layer of soil 1 foot thick and about 13 square miles in area 

would yield the estimated suspended-sediment discharge of Salt Creek 

at Lincoln.

The suspended-sediment discharge is generally most of the total 

sediment discharge for streams such as Salt Creek; however, some 

sediment not included in the measured suspended-sediment discharge 

may be transported either as bedload or as part of the suspended-sediment discharge in the unsampled zone near the streambed. A method 

devised by Colby (1957, p. 708-717) was used to compute the unmeasured sediment discharge at selected times on Salt Creek at Lincoln. The data in table 4 indicate that the measured sediment discharge is most of the total sediment discharge (measured discharge 

plus computed unmeasured discharge) over a wide range of water and 

sediment discharges.

The suspended sediment transported by Salt Creek is predominantly 

silt and clay, and the particle-size data shown in figure 11 represent 

water discharges ranging from 652 to 24,200 cfs.
H22 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

WATER DISCHARGE, IN CUBIC PERFEET SECOND

g° 

g 5 g°

g £° 0 

N

0 <

\

5

N

0

\

2

\

\

\

T

\

\

\

\

\

\

\

\

\

3

^^

**

0 5 0

^

7

^~

0

^^

^

^<^

9

~-~,

9

^^.

9S

^^.

8

~~-~^

10 20 40 60 80 90 95 98

PERCENTAGE OF TIME

99.5 99.9 99.99

FIGURE 10. Flow-duration curve, Salt Creek at Lincoln, 1950-59.
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H23

100

% o o o "o o o "o'o°

SAND

FIGURE 11. Percentage of sand, silt, and clay in suspended-sediment samples, Salt Creek

at Lincoln.

TABLE 4. Measured suspended-sediment discharffe, total sediment discharge, 

and hydraulic data for selected dates at Salt Creek at Lincoln, Nebr.

Date

1951

Apr. 22.. ___ _ 

Apr. 25............ ........... .-

M&y 31.. ......................

1954

June 9.. _____________

June 17-. ____________

Aug. 8 _ 

Aug. 23. 

Discharge

(cfs)

652

2,860

3,430

3,110

2,760

11,800

1,930

4,180

Suspended sediment

Discharge

(tons per

day)

16, 300

187,000

139,000

319, 000

93,200

436,000

16,500

62,000

Concentration

(ppm)

9,250

24,200

15,000

36,600

12,500

13,700

3,170

5,490

Total

sediment

discharge

(tons per

day)

16,650

189, 100

141,000

323,600

94,900

443,400

17,080

64,000

Mean

velocity

(fps)

2.20

2.75

2.39

3.04

2.54

3.57

1.86

2.73

Mean

depth

(ft)

1.96

4.53

6.15

7.05

4.60

12.75

4.30

6.60

Width

(ft)

169

231

234

237

237

255

236

234
H24 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES 

CHEMICAL QUALITY OF THE WATER

As water falls through the air and percolates through the soil, it 

absorbs carbon dioxide and becomes an effective solvent for many of 

the minerals in the earth's crust. The kinds and amounts of minerals 

dissolved by the water depend mainly on the types of minerals with 

which the water has contact and on the length of time of contact. 

Therefore, water that travels rapidly over the land does not ordinarily 

become as mineralized as water that infiltrates slowly through the 

ground.

Analyses of water from the Salt Creek basin were studied to determine the relations between water quality and geology and to evaluate the suitability of the water for domestic, industrial, and irrigation 

uses.

GROUND WATER

Large variations in the quality of water from an individual well 

are not common. Waters from different aquifers or from different 

parts of the same aquifer, however, are commonly different in chemical 

quality. The quality of the ground water in the Salt Creek basin was 

determined from analyses of samples representative of the three major 

sources of supply. Results of analyses are given in table 5.

The location of wells is shown in this report by numbers and letters. 

(See fig. 12.) The first number indicates the township; the second, 

the range; and the third, the section. The first lowercase letter following the section number indicates the quarter section; the second, 

the quarter-quarter section; and the third, the quarter-quarter-quarter 

section. These letters are arranged counterclockwise and begin with 

"a" in the northeast quarter. If more than one well is within the 10- 

acre tract, an additional number follows the lowercase letters.
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H25

RANGES EAST 

345 6 7

z 

<

o 

cc

UJ

5 \

\

\

\

\

13

12

11 E

o

z 

10 

tn

9 * 

w

2

8?

1-

1

BASELINE \

18

19

30

31

17

20

29

32

R. 6 E.

16

21

28

33

10

15

22

27

34

14

23

26

35

12

13

24

25

36

Well 9-6-5ddd

FIGURE 12. Well-numbering system.
H26 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

TABLE 5. Chemical analyses of ground 

[Use: D, domestic; Ind., industrial; Irr., irrigation; N., none; O, observation; PS,

Location

9-6-4db ...

36d ..

10-6-26b

I

5

17

40.5

36

72

8

P

D

D

O

Ind

Date of 

collection

May 24, 1951-

May31, I960..

May 24, 1951-

JunelO, 1950..

Temperature (°F)

CO

56

56

Silica (SiOa)

38

15

24

30

Iron (Fe)

1.2

.14

7.0

.06

«? 0

O

147

111

82

222

"55

a

41

15

20

63

'o?

5,

153

62

135

570

g

8

5.0

i a

5.3

7.6

Bicarbonate (HCOs)

Alia

456

350

638

280

Sands and gravels

7-6-19a ...

8-6-28dd-._..__

8-7-17CC 

33ad .

9-6-5d.. .......

10-6-18ab......

10-7-3bc.. ..

4d.. ......

5dbl......

5dda......

8aa. ......

ll-4-8aa 

ll-5-3aa. ......

ll-6-6b.. ......

29ba...... 

31a 

35c 

11-7-30C........

ll-8-17d.. 

12-9-2ac .....

32c _

13-4-19bb . 

13-5-22aa _ ...

13-10-19ccd-...

14-5-12ac.......

14-7-3db.......

14-8-lbc.......

2ba 

23da...... 

26aba..... 

l4-9-18cbc..... 

19da......

( 1350 

i «380

I »380

80 *40

42

30

25

63 *35

*100

396 *105

45

30.5

190 <25

91

73

108

392

180

85

123

118

122

130 

122 

110 

103

T 

T

T

PS

N

PS

T

D, S

D

D

T

T

Ind

PS

T

D

D 

D

D

D

Irr

PS

PS

PS

PS

PS

D

PS

D

.D

D

D 

D 

D 

D

Dec. 13, 1955. . 

Dec. 14, 1955..

 ..do......

May31, I960..

 ..do .. ...

 - do ... ..

Junel, 1950...

 do ......

 -do ... ...

Apr. 26, I960. .

June 27, 1951. .

1948 

Mar. 29, 1945-

May24, 1948..

May 31, 1950..

May 23, 1951- 

May25, 1950..

Dec. 30, 1955..

May 25, 1950-

 -do 

Sept. 26, 1952-

Tnltr f> 1QP19

May 29, 1951..

July 2, 1952 

Jan. 8, 1957 

Oct. 8, 1957 

May 13, 1958- 

Junel2, 1956.. 

Mar. 8, 1957... 

Feb. 11, 1958..

52 

51

55

57

57

54

57

57

61

53

57

54

60

55 

56

82

58

54

55

54

66

K.Q

65

EO

54

56 

55 

50 

55

26 

33

28

23

32

41

53

24

9.4

22

45

22

27 

34

26

22

41

26

45

40

24

45

32

43

43

53

43 

48 

40 

41

2.4 

.72

.12

.16

.14

5.5

1.0

9 A

.12

1.3

4.4

".12

.12

.12

1.7

1 9

09

.02

.05

.16

.10

3.9 

.07 

.23 

.66

292

79

111

125

115

49

150

124

44

22

42

50

46

118

181 

142

116

73

58

74

88 

102

55

47

79

83

QA

on

40 

52 

86 

59

95 

on

13

32

27

13

28in

10

9.0

14

20

8.5

20

36 

25

29

21

12

18

29 

21

10

23

17

17

17

13

12 

11 

16 

12

1,890 

w

47

63

58

108

74

81

32

7f

148

7

1(

245

4fi

380 

143

1,1

116

45

29

31

21 

12

32

20

34

2

2

3

1 

2 

2 

2

9.7 

4.4

3.8

3.2

5.4

3.4

11

5.2

2.6

>5

2.9

6

)3

9.6

4.3

8.3

6.2

80

8.4

3.8

7.8

5.3

11 

5.4

8.0

5.6

4.3

7

7

2

8 

0 

7 

4

382 

373

419

412

360

384

538

365

110

481

288

207

452

508

376

460 

445

480

466

326

220

372

432 

376

202

234

324

302

309

349

170 

215 

313 

237

Dakota group of

9-6-4cbd _ 

5dd ...

10-5-22dc-.- 

23cc... ....

26ab...... 

10-6-2dc..._._.

21bd...... 

26aab ..

26ab..-.- 

26ab2._.__ 

26bdd»...

10-7-5ada._____ 

6b_._ 

13bd...... 

18dc......

31babl_.__

f 55 

i 99 

I 151 

*2,000 

95

85 

187 

*2,650

143 

159

140 

*180 

80 

*192 

141.5

T 

T 

T 

N 

D 

PS 

D 

D 

N 

Ind 

Ind 

Ind 

Ind 

T 

T 

D 

Irr 

PS

July 1939-. .

.....do . .

Aug. 8, 1959... 

Jan. 28, I960 

May 20, 1953. .

Dec. 5, 1949...

Nov. 19, 1951-

Or»f 17 1Q*tQ

Apr. 24, 1951 .- 

 -do -

Oct. 17, 1959 

June 29, 1951 ..

July 6, 1950 

May 9, 1955 

August 1951 

61

54

60

58 

60

57

54 

56 

55

9.8 

37 

19 

19 

41 

9.6 

30

17 

22 

30

13 

16 

28 

23

25

.02 

.98 

3.3 

3.4

.11

.16

"2.1"

.06 

.04 

.07

82 

126 

147 

183 

77 

41 

78 

140 

184 

147 

415 

298 

347 

285 

263 

66 

62 

56

0.4 

17 

18 

143 

16 

14 

16 

2.6 

145 

152 

205 

122 

140 

135 

124 

14 

13 

14

48 

V 4,5 

9,990 

36 

460 

109 

137 

9,410 

5,6 

16, 100 

8,660 

9,5 

11,900 

10,600 

33 

68 

30

!8 

HO 

SO 

35 

6.1 

7.6 

7.2 

7.1 

98 

40 

17 

11 

S60 

44 

53 

3.6 

3.7 

4.0

123

"448" 

370 

322 

412 

390 

437 

407 

547 

419 

405 

763 

764 

286 

266 

239

1 Water from 360 ft. 2 Water from 260-270 ft. » Water from 290-300 ft. * Estimated.
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H27

water, Salt Creek basin, Nebraska

public supply; S, stock; T, test. Results in parts per million except as indicated]

Carbonate (COs)

Sulfate (804) Chloride (Cl) Fluoride (F)

6

1 !«

Dissolved solids

Calculated Residue on

evaporation 

180° Cat

Hardness CaCOss

Noncarbonate hardCaCOs ness asodium Percent 

Sodium-adsorptionratio

Specific conductance (micromhos percm 

25° C) at

aa

vium

oooo 175 

193 

18 

423

202 

10 

27 

893

0.8 

.2

.7 

_2

40 

.4 

.0 

116

0.14 

.30 

.25 

.30

1,020

2,450

1,100 

640 

636 

2,630

536 

339

288 

772

162

52 

0 

542

38

50 

61

2.9 

1.5 

3.4

8.9

1,610 

884 

981 

3,980

7.2 

7.1 

7.4 

6.8

of Pleistocene age

0 

6

0

0

0

13

0

0 

0

0

0

0

0

0

0

0 

0

0 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

617 

54

47

83

116

13

142

188 

18

193

48

61

49

126

91

110 

49

280 

114

60

40

20

37

44

83

68

46

47

96

33

23

25

45

40

3,030

7.5

16

52

35

44

46

51

84

820

87

67

5.0

115

46

655 

192

1,680 

110

16

20

6.0

7.5

6.0

8.0

6.0

15

15

3,5

1.5

3.8

5.0

16

5.5

1.6 

.3

.2

.3

0

.3

.3

.3

.2

.9

.2

.6

.8

.3

.4 

.2

.4 

.2

.4

.2

.2

.3

.3

.4

.2

.2

.5

.3

.5

.4

.2

.5

.5

2.7 

.1

25

130

84

1.1

83

32

.6

1.2

.2

.4

35

2.5 

131

5.3 

3.2

6.2

28

.7

.7

14

.5

.0

20

21

4.3

.5

21

11

13

4.2

0.50 

.01

.13

.30

.37

.08

.20

.20 

.30

.15

.25

.23

.18 ~M6~

.07

.12

.30

.08

.11

.06

.13

.10

.08

.09

6,150

716

1,630

3,390

6,350 

424

546

730

658

480

958

1,010 

318

504

404

830

622

1,780 

972

3,670 

862

408

352

370

448

434

336

328

406

415

455

382

257

277

417

305

1,120 

317

331

398

177

490

433 

151

90

92

162

207

150

377

598 

458

502 

409

269

194

259

338

342

180

212

268

277

304

255

148

176

279

196

807 

11

0

106

103

0

49

134 

61

0

0

0

0

0

69

221 

93

108 

27

2

14

0

0

34

14

20

2

29

51

0

9

0

22

2

78 

17

23

33

24

56

24

29 

31

95

77

50

52

7fi

21

58 

40

84 

38

26

24

20

11

7

27

16

21

18

16

21

91

19

17

21

25

.7

1.1

1.3

1.3

3.5

1.5

1.7 

1.1

35

6.7

2.6

3.1

8.7

1.0

6.7 

2.9

23

2.5

1.2

.9

.8

.5

.3

1.0

.6

.9

.7

.7

.9

.6

.7

.7

.8

10,300 

663

1,120

806

1,060

949

765

1,130

1,070 

477

3,500

836

682

766

1,310

894

2,790 

1,490

6,210 

1,190

621

509

575

696

673

492

483

647

630

661

590

374

427

634

467

7.9

8,2

72

73

7 4

84

7 5

7.1

fi 8

7 2

7 2

8 2

7,3

7 0

7.2 

7 6

7.4 

7,5

7 1

7.1

7 3

74

7.4

7.5

8.0

7,3

7.9

7.3

7,4

7.0

7.6

75

7.1

Cretaceous age

0 

0

0 

0

0

0 

0

0 

0 

0

0 

0 

0

0

0

99

471

826

3,150 

16

68 

29

18

2,950 

1,250

2,280 

1,340 

1,790

2,570 

2,280 

50

44

42

748

3,610

6,200

13,800 

11

590 

101

314

13,200 

8,080

24,400 

12,800 

13,900

16,700 

15, 100 

13

71

14

2.4 

.4

.2 

.2

.1

2.4

2.3

2.2

.9 

1.7 

.3

.2

.1

2.9 

7.4

.6 

.0

.8

10

32 

35

21 

.3 

1.6

1.7

9.6

5.5 

.10

.34

.07

3.5

.83 

.69

4.8 

4.1 

.30

.11

27,500

1,360

26,200 

15,400

43,800 

23,500 

25,800

32,000 

28,800

28,200 

389

1,360

597

945

26,600 

16 ''OO

43,800 

23,700 

26,700

32, 100 

29,100 

348

422

336

206

384

439

1,040 

259

159 

261

456

1,050 

995

1,880 

1,250 

1,440

1,270 

1,170

222

208

196

105

673 

0

0 

0

136

692 

661

1,430 

906 

1,110

644 

544 

0

0

0

84

93

95

95 

23

86 

47

39

95

92

95 

94 

93

95 

95

34

41

25

15

53

88

134 

1.0

16 

2.9

2.8

126 

76

164 

108 

107

146 

135 

1.0

2.0

.9

38,000 

626

2,470 

1,010

1,560

38,900

62,700 

36,100

45,800 

43,000 

540

707

500

7.4 

6.9

7.6 

7.5

7.8

6.9 

7.2

7.0 

7.0 

6.8

7.1 

8.1 

7.1

7.1

7.0

5 From analysis by Layne Research Div., Memphis, Tenn.
H28 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES 

WATER FROM THE 1>AKOTA GROUP

The quality of ground water and surface water in parts of the basin 

is affected by the Dakota group, which characteristically yields water 

that contains large amounts of dissolved solids principally sodium 

and chloride. However, most of the salts have been leached from 

some parts of the Dakota, and water from these parts is relatively low 

in dissolved solids.

Most of the available data on the chemical quality of water from 

the Dakota group are for wells in and near Lincoln, where in places 

the Dakota is at or near the surface. The water from most of these 

wells was of the sodium chloride type and contained high concentrations of dissolved solids. (See table 5.) The water from some of 

the wells, however, was of the calcium bicarbonate type and contained 

less than 500 ppm of dissolved solids; such water generally overlies 

water containing higher concentrations of dissolved solids.

The data indicate that, in places, the concentration of dissolved solids 

increases with depth; for example, the concentration of chloride in 

the water from test hole 9-6-4cbd increased from 748 ppm at a depth 

of 55 feet to 6,200 ppm at 151 feet. Therefore, the rate of pumping 

can affect the quality of the water obtained, particularly if the rate 

is high for prolonged periods; the water level can be lowered so much 

that the wells begin to yield salty water. Before 1933 the water supply 

of Lincoln was obtained in the city limits from about 20 wells that 

could produce a combined total of 10 million gallons per day for short 

periods. Some of these wells, however, began to produce salty water 

and were abandoned. Since 1933, the city of Lincoln has been supplied principally by water from a well field near Ashland. Some of 

the wells in the city limits are used during periods when the demand 

for water is exceptionally high.

Figure 13 shows diagrammatically (Stiff, 1951) the relations of 

dissolved solids to chloride and to water type. The water from the 

Dakota group as represented by analyses in table 5, has either a fairly 

low or an extremely high dissolved-solids content. As the dissolvedsolids content increases, the water type changes from calcium bicarbonate to sodium chloride, and the concentration of chloride 

increases. In waters that contain more than about 900 ppm of dissolved solids, the amount of chloride increases almost proportionally 

with the increase in dissolved solids.

At some places, water from the Dakota issues from springs and 

adversely affects the quality of the surface waters, especially when 

stream discharges are low. Also, at some places, infiltration of water 

from the Dakota adversely affects the quality of the adjacent waterbearing deposits.
a3d siavd NI 'sanos QBAIOSSIQ
H30 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES 

WATER FROM THE SANDS AND GRAVEL OF PLEISTOCENE AGE

Most of the water for domestic, industrial, and irrigation uses in the 

basin is from sands and gravels of Pleistocene age of variable thickness and extent. In the southern half of the basin, the deposits are not 

capable of yielding the large quantities of water required for the 

city of Lincoln; therefore, Lincoln has developed its supplies in the 

deposits east of Ashland in the Platte River valley.

Dissolved solids in the water from the sands and gravels of Pleistocene age were generally less than 1,000 ppm in the southern half of 

the basin and less than 500 ppm in the northern half. Locally in 

the southern half the dissolved solids were higher than 1,000 ppm. 

(See table 5.) In test hole 7-6-19a, the dissolved solids were 424 ppm 

at a depth of 260 to 270 feet, about 800 ppm (estimated) at 290 to 300 

feet, and 6,350 ppm at 350 feet. Water from the Dakota evidently has 

infiltrated into the deep sands and gravels because the increase in 

dissolved solids was due principally to increases in sodium and chloride. Except where water from the Dakota affects water in the sands 

and gravels of Pleistocene age in the southern half of the basin, the 

water is of the calcium bicarbonate type. Concentrations of iron are 

greater than 1 ppm in water from many of the wells.

WATER FROM THE AIXUVIUM

The alluvium in most of the basin does not yield large quantities 

of water, although in a few places, such as near Ashland, some wells 

have produced enough water for irrigation. Not much information 

on the quality of water in the alluvium is available (see table 5); however, the water probably is of the calcium bicarbonate type and has 

less than 1,000 ppm of dissolved solids, except where water from the 

Dakota has infiltrated the alluvium, such as in the vicinity of well 

10-6-26b.

SURFACE WATER

Streamflow consists of both overland flow and effluent from the 

ground-water reservoir. If the chemical composition of the overland 

flow differs significantly from that of the ground-water effluent, the 

chemical composition of the streamflow will vary with changes in 

discharge. When the discharge is high, the chemical quality of the 

streamflow is similar to that of the overland flow; when the discharge 

is low, the chemical quality of the streamflow is similar to that of the 

ground water.

Most of the analyses in table 6 are representative of low discharge. 

The water in the upstream parts of Salt Creek and its tributaries is 

similar to the water from sands and gravels of Pleistocene age; it is 

of the calcium bicarbonate type and contains about 600 ppm or less
TABLE 6. Chemical analyses of surface water, Salt Creek basin, Nebraska Og 

[Results in parts per million except as indicated] 2

>3t

Date of collection Discharge (cfs)

Silica (SiOj)

Iron (Fe)

Calcium (Ca)

Magnesium (Mg) Sodium (Na) (K) Potassium 

Bicarbonate (HCO )3

Carbonate (CO )3

Sulfate (SO)4

Chloride (Cl) Fluoride (F) Nitrate NO)3

s

2o

Dissolved solids

Calculated

Residue at 

180°C

fees a.2

11

PH

Tons per acre-foot

CaCO Hrdness as3

Noncarbonate hardness 

CaCOas sodium Percent 

1 

g "a 

§

03

aa

02

Specific conductance 

(micromhos at percm

25° C)

MENTATION, QUALE

Hd

Salt Creek, near Saltillo School K!

May 23, 1951 .... 12 0.08 56 13 29 211 0 59 12 0.5 3.8 0.06 304 0.41 193 20 25 0.9 475

O 

7.4 ^

- ( <s

Salt Creek, above confluence of Haines Branch > 

H

May 24, 1951---.-- 11 0.06 53 15 30 211 0 60 12 0.3 4.4 0.07 314 0.43 192 19 25 0.9 479 7.5 Jfl

00 

Haines Branch, 3% miles south of Emerald > 

122 16 55 394 0 141 16 616 0.84 372 49 24 1.3 889

» '

Haines Branch, above confluence with Salt Creek S

May 24, 1951 _ . 20 0.05 136 32 205 438 0 168 270 0.4 2.6 0.14 1,050 1,120 1.52. 472 113 49 4.1 .1,700

f*l

8.0 ~

a

H 

Salt Creek, downstream from Haines Branch fcj

Hrt

May 25, 1950 .... 21 0.06 89 20 112 300 0 102 135 0.4 5.6 722 0.98 305 59 44 2.8 1,050 7.4
[Results in parts per million except as indicated]

(8ON) a^Bflijsi

«)»P, M

(£OS) awing

(8QO) a^uoq^o

(8OOH) a^enoqoBOia;

(3) ranjssBjoj

(BN) tnnjpog

ow-p w

(BO) nmjofBo

(aj[) uojj

(ZOIS) eojlig

"3

1 a

«-^«

§c

a i

s 

te

 31

oosi0o

01 w

 81

 s

5a0sai1os§o

CO

os'

Oak Creek, 1 milesouth ofRaymond

t 1 s5

t-o<"

i

3^I

1 11

gf

1 

too§68sioS

53

tc5

OS

IM

Oak Creek, near WestLincoln

^0sss

COoS10

IQ 

CO

03

sf
Salt Creek, at Lincoln

GO

TVTflv Q 1Q*ift

Do.... ... ...

May 23. ...........

May 23, 1951. 

May 20, 1953.. _ ..

May 27. ______

July3, 1956 

July 10, 1958-....-

26,500 

1 16, 700 

98 

137 

178 

915 

3,840 

18,500

12 

13 

30

24

0.04

.01

12 

11 

108

102 

36 

16

2.7 

2.3 

32

32

8.5 

4.4

22 

23 

1,080 

1,100 

985 12 

226 7.8 

56 4.4 

21

54 

47 

357 

282 

388

96 

106

0 

0 

0 

0 

0

0 

0

17 

18 

245 

255 

230

6.8

17 

20 

1,560 

1,600 

1,420

23

0.5 

.5 

.5

.1

1.5 

1.5 

6.6

8.0

.8

0.20 

.10

.32

.33

3,240

3,000

U4 

124 

3,340

3,000 

764 

241 

167

0.16 

.17 

4.54

4.08 

1.04 

.33 

.23

41 

37 

401 

366 

386 

125 

58 

74

0 

0 

108 

135 

68

0 

0

53

58 

85 

87 

84 

78 

66 

36

1.5 

1.7 

24 

25 

22 

8.8 

3.2 

1.1

172 

170 

5,460 

5,560 

5,250 

1,390 

428 

259

H 

74 O

7.4 a

7.4 £j 

7.2 « 

8.0 3 

69 ^ 

7.1 g

6.9 HH

O'4 

Little Salt Creek, 8 miles north of Lincoln

Feb. 26, 1952 _ .... 1,310 3,110 4.23 458 5,250

f->d

>M

Little Salt Creek, 4 miles north of Lincoln H

Feb. 26, 1952 2,360 5,140 6.99 520 8,580 0

*]

Salt Creek, west of Waverly ^

^

May 23, 1951. 15 0.05 83 23 588 275 0 190 816 0.8 2.1 0.30 1,850 1,860 2.53 300 74 81 15 3,160

^

7.4 H

so

Wahoo Creek, near Ashland gj

h».

18 0.01 90 26 112 346 0 158 87 0.7 1.7 0.20 680 0.92 330 46 43 2.7 1,120 7.8 H

Salt Creek, near Ashland <#

May 23, 1950. 24 0.02 91 23 484 300 0 142 688 0.4 12 1,610 1,820 2.48 322 76 77 12 2,790

H 

7.3 ^W

i Daily mean discharge. gj 

td 

»

W COCO
H34 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

of dissolved solids. The water in the vicinity of Lincoln is similar 

to the water from the Dakota group; it is of the sodium chloride 

type and contains more than 1,000 ppm of dissolved, solids.

Partial analyses indicate that the water in Little Salt Creek during 

periods of low discharge is high in dissolved solids and is probably of 

the sodium chloride type. Saline soils are fairly common in the 

downstream two-thirds of Little Salt Creek valley and reflect both 

the quality of water and the poor drainage in parts of the flood plain. 

Some very small areas completely devoid of vegetation were observed. 

The bare areas were fringed with scattered saltwort that graded into 

saltbush; a little farther out the saltbush graded into saltgrass and 

western wheatgrass.

Figure 14 shows diagrammatically the increases in the concentrations of dissolved solids and chloride as the water in the streams becomes affected by the water from the Dakota. As the water in Haines 

Branch (3 and 4) and in Oak Creek (8, 9, and 10) moves downstream, 

the concentrations of sodium chloride increase to such a degree that 

the water type changes from calcium bicarbonate to sodium chloride. 

Downstream from Lincoln, concentrations of dissolved solids and 

chloride in Salt Creek decrease somewhat, but the effects of the water 

from the Dakota are still noticeable at Ashland. The underlying 

bedrock in most of this reach of Salt Creek consists of limestones 

and shales of Pennsylvanian age.

The dissolved-solids content in the water from Salt Creek at Lincoln decreases as the discharge increases, and the water type changes 

from sodium chloride at low discharge to sodium bicarbonate at high 

discharge. (See fig. 15.)

WATER QUALITY AND USE

Water supply is of prime consideration in the growth of either an 

industrial or an agricultural economy. The use of the available water 

for specific purposes, however, may be restricted by the amounts and 

kinds of dissolved material in the water. For some uses the water 

must meet strict quality standards.

Nearly all the water used in the Salt Creek basin for domestic, public, industrial, and agricultural supplies is produced from wells; 

surface water of adequate quantity and quality is not available. Surface water, however, is used for pollution abatement, recreation, and 

some livestock needs.

DOMESTIC AND PUBLIC SUPFMES

Water for domestic and public supplies should have no unpleasant 

odor or taste, be free from sediment and color, and contain no pathogenic organisms or excessive quantities of minerals. Standards have
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H35

FIGTJBB 14. Concentrations of dissolved solids and chloride in surface water during periods 

of low discharge, Salt Creek basin. Explanation : 1, Salt Creek near Saltillo School; 2, 

Salt Creek above confluence of Haines Branch; 3, Haines Branch, 3% miles south of 

Emerald; 4, Haines Branch above confluence with Salt Creek; 5, Salt Creek downstream 

from Haines Branch; 6, Middle Creek near Emerald; 7, Salt Creek south of Oak Lake; 

8, Oak Creek, 1 mile south of Raymond; 9, Oak Creek near Oak Valley School; 10, Oak 

Creek near West Lincoln; 11, Salt Creek at Lincoln; 12, Little Salt Creek, 8 miles north 

of Lincoln; 13, Little Salt Creek, 4 miles north of Lincoln; 14, Salt Creek west of 

Waverly ; 15, Wahoo Creek near Ashland ; 16, Salt Creek near Ashland.
- 

i'ii 

O

CD

7

z

NI 'sanos a3Aiossia
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H37

been established by the U.S. Public Health Service (1961) for drinking water used on interstate carriers and should be applicable to all 

public water supplies in the United States. Some of these standards 

for the chemical constituents of the water are as follows:

Recommended 

Constituent maxcimum

(ppm) 

Iron (Fe)_____________________________________ 0.3

Manganese (Mn)________________________________ . 05 

Lead (Pb)____________________________________ *. 05 

Arsenic (As) ___________________________________ \ 01 

Sulfate (SO4 ) ___________________________________ 250 

Chloride (01)___________________________________ 250 

Fluoride (F) ______________________________ _ 1Z 1.3 

Dissolved solids__________________________________ 500

1 Mandatory.

8 Based on long-term annual average of maximum daily air temperatures at Lincoln, 

Nebr.

The standards for lead, arsenic, and fluoride are mandatory because 

these constituents in sufficient quantity are toxic to human beings. 

According to Welsh and Thomas (1960), excessive amounts of arsenic 

may cause chronic arseniasis, which is characterized by small eruptions 

on the hands and feet; and excessive amounts of fluoride may cause 

fluorosis or "mottled enamel" of children's teeth. In most natural 

water the concentration of these constituents is low. Studies have 

shown, however, that fluoride in concentrations between 0.6 and 1.2 

ppm in drinking water have a beneficial effect on children's teeth.

Excessive concentrations of iron and manganese in the water stain 

fabrics and porcelain or enamelware, produce unsavory flavors in 

coffee and tea, and discolor vegetables during cooking. Micro-organisms, which thrive in water containing iron, may cause disagreeable 

tastes and odors in the water. Magnesium and sulfate in high concentrations in water may have a laxative effect on some people and 

cause an unpleasant taste, and large quantities of chloride in water 

may cause a salty taste.

Nitrate is an end product in the decomposition of organic wastes; 

therefore, high concentrations of nitrate may indicate pollution of the 

water. Maxcy (1950, p. 265) reported that water containing more 

than 44 ppm of nitrate should be regarded as unsafe for infants because it may cause cyanosis.

Hardness is caused principally by calcium and magnesium in water. 

It impairs the quality of the water because of curd that forms when 

soap is added and because of scale that is deposited in water pipes, 

heaters, and boilers. No standards for hardness have been established, 

but the following gradations are generally recognized:
H38 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

Hardness as CaCOa, 

Inppm

<60___ ________

60-120--__--_-

121-200-------

>200-____ -_

Rating

Soft _--_-_-______._

Hard

Suitability

Suitable for many uses without

further softening. 

Usable except in some industrial

applications. 

Softening required by laundries and

some other industries. 

Requires softening for most uses.

The analyses in table 7 indicate that the water from most public 

supplies is very hard but contains less than 500 ppm of dissolved 

solids. Iron and manganese in many of the supplies and chloride 

in one analysis exceeded the maximum concentrations recommended 

by the U.S. Public Health Service (1961). High concentrations of 

nitrate indicated possible pollution of the water from three of the 

supplies.

INDUSTRY

In industries, the quality requirements for water depend on the 

specific use of the water. The requirements for water used for cooling 

or waste disposal are not so strict as those for water used in processing 

or incorporated in the final product. Generally, water that is of satisfactory quality for domestic and public supply is also satisfactory for 

many industrial uses or can be made satisfactory with a reasonable 

amount of treatment. Table 8 shows the water-quality tolerances 

for some industrial uses (American Water Works Association, 1950).

IRRIGATION

The amount of precipitation is sufficient for successful dryland 

farming, except during the growing season in some years. Recently, 

however, ground water has been used for irrigation, particularly in 

Salt Creek basin northeast of Lincoln and in Wahoo Creek valley. 

According to the Conservation and Survey Division, University of 

Nebraska,, there were 208 irrigation wells in Lancaster and Saunders 

Counties in 1958; most of them were in Salt Creek basin. Although 

many applications for the use of surface water have been filed with 

the Nebraska Department of Water Resources, little of the surface 

water in the basin is used for irrigation. Streamflow is generally low 

when the need for irrigation is the greatest.

Water used for irrigation should be of such quality that it will not 

adversely affect the productivity of the land to which it is applied. 

The suitability of the water for irrigation, however, depends not only 

on the quality of the water but also on such conditions as climate, 

soil structure and drainage, type of crop, and farm-management
SEDIMENTATION, QUALITY OP WATER, SALT CREEK, NEBR. H39

practices. Methods have been suggested for classifying irrigation 

water so that its long-term effect on soil productivity can be forecast (Wilcox, 1948; Scofield, 1936; Eaton, 1950; U.S. Salinity Laboratory Staff, 1954). The method used in this report was proposed by 

the U.S. Salinity Laboratory Staff (1954).

Properties of principal importance in determining the suitability 

of water for irrigation are the total concentration of the dissolved 

salts, the relative proportion of sodium to calcium and magnesium, 

the concentration of boron or other elements that may be toxic, and 

the concentration of bicarbonate as compared with the concentrations 

of calcium and magnesium.

High concentrations of dissolved salts in irrigation water may 

cause an accumulation of salts in the soil solution and may make 

the soil saline. Because all plants absorb water by osmosis, a favorable balance must be maintained between salts within a plant and 

salts in the soil solution. When the total concentration of salts in 

the soil solution becomes too high for plants to get an adequate amount 

of water or when the concentration of certain salts in the soil solution 

becomes so high as to be toxic, the growth of the plants is adversely 

affected. The tendency of irrigation water to cause an accumulation 

of salts in the soil is called the salinity hazard of the water. The 

specific conductance of the water is used as an index of the salinity 

hazard.

High concentrations of sodium relative to the concentrations of 

calcium and magnesium in irrigation water may change soil structure. 

Cations in the soil water become fixed on the surface of fine soil 

particles; calcium and magnesium tend to flocculate the particles, 

whereas sodium tends to deflocculate them. Flocculation gives the soil 

looseness, provides good penetration by water and air, and generally 

gives the soil good tillage properties. Deflocculation promotes packing and prevents free movement of air and water. The adverse effect 

on soil structure caused by high sodium concentrations in the irrigation 

water is called the sodium hazard of the water.

An index used for predicting the sodium hazard of a water is the 

sodium-adsorption-ratio (SAR), which is defined by the equation

SAR=-

2

where Na+1, Ca+2, and Mg+2 are in equivalents per million (U.S. Salinity Laboratory Staff, 1954).
TABLB 7. Chemical analyses of water from public supplies, Salt Creek basin, Nebraska

[Analyses by Nebraska Department of Health. Results in parts per million except as indicated. Point of collection: D, distribution system; 8, source]

w

Municipality

Ashland (well 1) ».... __

Ashland (well 2) »... ......

Ashland (well 3) »._.__..__

Brainard ..................

Cedar Bluffs _______

Do ...... . -.

Colon.. _________ _

Davey. ______ ........

Denton ____ ...........

Do.. ...............

Dwight »_._ __ . .........

Do. » _________ .

Eagle (east well). .........

Emerald '.. ...............

Greenwood » ..__.. .....

Do. «- ._.. -

Hickman (well 1) ... .

Hickman (well 2) ' ____

Lincoln __ _ __ .....

Do.......... .......

Do. ....... ......

Point ofcollection

S

S

s

s

s

s

s

s

3

D

S

S

s

s

D

D

S

S

s

s

D

D

D

D

Depth well (feet) of 

74

73

100

324

116-140

93

95

110

160+

376

376

244

396

106

106

265

45

38

Date of 

collection

8-13-57

8-13-57

8-13-57

8- 8-52

5- 9-57

8- 9-55

9-11-56

12-17-57

5-16-56

12- 8-52

2-23-56

2-8-57

9-27-54

2-14-55

5-23-55

' 4-12-55

'5-14-58

Iron (Fe)

0.1

.0

.0

.1

.5

.0

.3

1.9

.2

8.5

1.1

2.1

1.3

1.1

.1

.05

.0

.4

1.3

.05

3.1

.01

.01

.06

.04

Manganese (M)

0.1

.2

.1

.54

.3

.0

.01

.40

.0

.27

.4

.57

.24

.0

.24

.01

.05

.35

.02

.55

.0

.01

1Lead (Pb) 

0

0

0

0

Arsenic (As)

0.004

.005

004

Calcium (Ca)

64

62

64

104

ftQ

81

a5

106

2

74

130

79

46

54

53

"55

S

1 

1

1Q

15

13

22

*yj

9*

12

21

5.6

99

34

20

21

12

11

Sodium (Na)

25

97

99

9

17

98

1

24

oo

OA

56

1

1

OQ

00

EC

35

70

on

g

^ ft

'o 

Hi

10

10

0

5

53

10

5

6

10

3

61

12

4

6

3

5.6

36

28

Bicarbonate (HCOs)

176

934

417

346

417

388

OCQ

322

351

434

161

351

456

371

OQQ

398

317

403

203

206

201

(COs) Carbonate 

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

(SOSulfate )4

64

40

52

163

on

fiQ

115

SO

4

130

106

55

44

135

KA

66

OQ

OQ

55

134

70

54

54

Chloride (Cl)

VI

1Q

14

5.7

11

85

112

1 Q

5

193

294

11

22

27

6.6

6.0

6.5

18

41

35

so

14

23

11

(F) Fluoride 

0.3

.4

.3

2

.1

3

.4

.2

.2

.2

.2

.2

.4

.2

.3

.3

.2

.4

.4

.5

(NO )Nitrate 8

<44

<T44 <'44

<r"44

40 <"44

<r"44

<'44

<^44

<44

<*44

<44 <"44

<<44

<"44

<"44

<"44

75

<T44

75

 £"44

3.5

2.4

(residue Dissolved solids

evaporation at on

105°C)

Aon

420

370

782

<tfifi

700

686

458 "W)

850

Q")fl

OQJ.

614

470

AQf\

377

356

7OJ.

7^4.

458

758

336 »319

>297

Hardness CaCOss

236

216

212

500

348

376

264

306

212

262

358

352

28

210

283

274

l^fi

464

280

47a

200

184

179

Noncarbonate hardness 

CaCOjs 

Q9

24

12

158

64

34

0

4

0

0

2

220

0

0

0

9A

W

14834

15

14

Percent sodium

ift

?0

18

4

10

36

56

14

?,4

62

10

?,6

93

54

ift

1Q

21

?,1

24

24

30

25

Sodium-adsorption-ratio

0.7

7

2

4

2 O

4 1

.6

1.0

5 3

.5

1 3

13

3,3

7

9

1.1

9

1.4

g

1,1

.9

W 

a

6 9

7.2

7 3

7.5

7.5

7 2

7.1

7 4

7 4

7,3

7.7

7.4

7.7

8,2

7.5

7.3

7.1

7,2

7,6

7,1

73

7,7

7.5
Mead (well 1)... . .........

Wahoo «. . ...... .......

Yutan (well 1) .........

D

S

S 

S 

D

D

S

S

s

D

S 

D

S 

S

65

72 

132

65

60

180 

80

80± 

144

4-21-53 

10-3-58 

5-20-58 

5-20-58

12- 5-51 

1-19-59 

6-23-59 

11-24-50

4-21-53

9-26-52 

2-24-53 

10-26-56

.0 

1.9 

2.0 

.5 

.05

.0 

7.3 

.0 

.49

1.2 

.0

.02 

.0 

.0

.0 

.5 

.2 

.0 

.05

.0 

2.5 

<.05 

.05

.0 

.0

.1 

.2

0

0

0 

0

0 

0

.01

.01

.012 

.02

.008 

.02

64 

104 

85 

93

88 

90

91

72

67

28 

19 

18 

18

23 

19

35

28

28

32 

26 

18 

21

I

31 

53

(

11 

32 

35 

18

3

,! 

g

36

16 

10 

8 

i4

4 

3 

11 

5 

6

346 

400 

.234 

312 

398

461 

239 

395 

393

381 

322 

359 

325 

200

0 

0 

0 

0 

0

0 

0 

0 

0

0 

0 

0 

0

0

37 

56 

24 

40 

54

145 

60 

32 

112

55 

50 

90 

38 

32

5.7 

6 

24 

2 

3.8

8.6 

30 

44 

13

3.8 

19 

28 

13 

9.6

.2 

.4 

.5 

.3 

.3

.3 

.2

.7 

.1

.3 

.3 

.3 

.2

<44

<44 

40 

<44

64 

<44 

<44 

<44

<44 

<44 

<44 

<44 

<44

404 

532 

558 

470 

416

656

490 

616

486 

438 

468 

406 

260

276 

336 

284 

304 

310

494 

316 

304 

384

370 

294 

330 

282 

132

0 

8 

92 

48 

0

116 

120 

0 

62

58 

30 

36 

16 

0

20 

14 

11 

12 

20

17 

17 

27 

16

6 

19 

18 

12 

37

.8 

.6 

.5 

.5 

.9

.9 

.8 

1.3

.7

.2 

.8

!s

1.4

7.3 CB 

7.4 W 

7.4 O

7.4 a 7- 3 5

7.2 %

"0 §

7.7 § 

7.2 ~ 

7.2 _

7 7.3 ^ fJd

>i-<

i See also table 5, well location 12-9-2ac. See also table 5, well location 8-7-33ad. £3 

2 See also table 5, well location 13-4-19bb. ' Analysis by U.S. Qeol. Survey. M{ 

s See also table 5, well location 10-5-23cc. 8 Residue on evaporation at 180°C. 

« See also table 5, well location ll-4-8aa. e See also table 5, well location 13-5-22aa. O 

« See also table 5, well location 12-9-32c. 10 See also table 5, well location 14-7-3db. *3

so

M

w
W

qual

for

[Limits in million parts except per as indicated]

spnos moj,

H*

(8OO«O

--P-H

jopo

(I/im) U98

paumsuoo

,0,00

^IIPIWL

Industry

conditioning Air ».- ........

|

OiOO 

eo"

00

oo oo os t> t*- 

CO

JjAII

? SS

w'

Cl

ss

S C

 H Ot

3 C

Boiler feed:

0-150 nsi-___ _

I

a

 z

S

S

Sg

00 ! !t2

1OO

e

1 

S

s

Illl -S

1O 

1O

0

o

C

250psiandup-_ ________ ...

Brewing: s 

Light ... , .....

ooc

Canning: Legumes. ________ .. Carbonated beverages 

d

C

rH

O 

_____

g

!

1

i

1

«0

C 1O

fa*

«-b.e 

5

N TO

clear, Pastics, uncolored 

e.

__

w C

C tS CJ

lO 

Paper and pulp: «« 

Groundwood---- 

Kraftpulp 

....... 

________

11 I

op 

eoo 

06

00

s

§§ °°§

eo

1C 1O 1O

Light HL-Grade paper, _ ...

(viscose) Rayon pulp:

ProductionManufacture 

__________ ......

______________

| 

3

S3

o NIA '

3 1010

Tanning » __ _____________ .. 

Textiles: 

General __ _ ..Dyeing"-. .................

^ 

1

§

SlO

Cotton bandage w 

10

______
1 American Water Works Association (1950).

8 A, No corrosiveness; B, No slime formation; C, Conformance to Federal drinkingwater standards necessary; D, NaCl, 275 ppm.

a Waters with algae and hydrogen sulfide odors are most unsuitable for air conditioning.

4 Some hardness desirable.

«Water for distilling must meet the same general requirements as for brewing (gin 

and spirits mashing water of light-beer quality; whiskey mashing water of dark-beer 

quality).

«Clear, odorless, sterile water for syrup and carbonization. Water consistent in 

character. Most high quality filtered municipal water not satisfactory for beverages.

7 Hard candy requires pH of 7.0 or greater, as low value favors inversion of sucrose, 

causing sticky product.

8 Control of corrosiveness is necessary as is also control of organisms, such as sulfur 

and iron bacteria, which tend to form slimes.

 CaCHCOs) 2 particularly troublesome. Mg(HCOs)2 tends to greenish color. CO2 

assists to prevent cracking. Sulfates and chlorides of Ca, Mg, Na should each be less 

than 300 ppm (white butts).

10 Uniformity of composition and temperature desirable. Iron objectionable as 

cellulose adsorbs iron from dilute solutions. Manganese very objectionable, clogs 

pipelines and is oxidized to permanganates by chlorine, causing reddish color.

11 Excessive iron, manganese, or turbidity creates spots and,discoloration in tanning 

of hides and leather goods.

18 Constant composition; residual alumina 0.5 ppm.

w Calcium, magnesium, iron, manganese, suspended matter, and soluble organic 

matter may be objectionable. I

I

ja

GO
H44 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

The salinity hazard and sodium hazard of the water may be evaluated by use of a diagram by the U.S. Salinity Laboratory Staff (1954). 

(See fig. 16.) Interpretation of the diagram is as follows:

I 10

5

- 6

o

O 

en 6

4567 8 9 1000

CI-S4

CI-S3

CI-S2

CI-SI

I I IT

C2-S4

C2-S3

C2-S2

C2-SI

C3-S4

C3-S3

C3-S2

t

3 I 4 567 8910.000 2

C4-S4

C4-S2

C4-SI

I I I I I I

250 750 2250 10,000 70,000 

SPECIFIC CONDUCTANCE (MICROMHOS PER CM AT 25 C C)

HIGH VERY HIGH

+ Alluvium

SALINITY HAZARD

EXPLANATION 

Pleistocene sands and gravels o Dakota group

FIGURE 16. Classification of water for irrigation. Diagram after U.S. Salinity Laboratory

Staff (1954).

Low-salinity water (Cl) can be used for irrigation with most crops on most 

soils with, little likelihood that soil salinity will develop. Some leaching is 

required, hut this occurs under normal irrigation practices except in soils of 

extremely low permeability.

Medium-salinity water (C2) can be used if a moderate amount of leaching occurs. 

Plants with moderate salt tolerance can be grown in most cases without special practices for salinity control.

High-salinity water (C3) cannot be used on soils with restricted drainage. Even 

 with adequate drainage, special management for salinity control may be 

required, and plants with good salt tolerance should be selected.
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H45

Very high salinity water (C4) is not suitable for irrigation under ordinary conditions but may be used occasionally under very special circumstances. The 

soils must be permeable, drainage must be adequate, irrigation water must be 

applied in excess to provide considerable leaching, and very salt-tolerant 

crops should be selected.

The classification of irrigation waters with respect to SAR is based primarily 

on the effect of exchangeable sodium on the physical condition of the soil. 

Sodium-sensitive plants may, however, suffer injury as a result of sodium accumulation in plant tissues when exchangeable-sodium values are lower than 

those effective in causing deterioration of the physical condition of the soil.

Low-sodium water (Si) can be used for irrigation on almost all soils with little 

danger of the development of harmful levels of exchangeable sodium. However, sodium-sensitive crops such as stone-fruit trees and avocados may 'accumulate injurious concentrations of sodium.

Medium-sodium water (S2) will present an appreciable sodium hazard in finetextured soils having high cation-exchange capacity, especially under low-leaching conditions, unless gypsum is present in the soil. This water may be used 

on coarse-textured or organic soils with good permeability.

High-sodium water (S3) may produce harmful levels of exchangeable sodium 

in most soils and will require special soil management good drainage, high 

leaching, and organic-matter additions. Gypsiferous soils may not develop 

harmful levels of exchangeable sodium from such waters. Chemical amendments may be required for replacement of exchangeable sodium, except that 

amendments may not be feasible with waters of very high salinity.

Very high sodium water (S4) is generally unsatisfactory for irrigation purposes 

except at low and perhaps medium salinity, where the solution of calcium 

from the soil or use of gypsum or other amendments may make the use of 

these waters feasible.

In the Salt Creek basin most of the water from the Dakota group 

is unsatisfactory for irrigation because both the salinity hazard and 

the sodium hazard are very high. Some of the water is suitable for 

irrigation, but such water is insufficient for large-scale development. 

Most of the water from the deposits of Pleistocene age and the alluvium can be used for irrigation if drainage is adequate and if salttolerant plants are grown. In some places the water is unsatisfactory 

for irrigation, because it has been contaminated by the water from 

the Dakota.

Boron is essential to the normal growth of all plants; however, if 

present in excessive concentrations, it may be highly toxic to some 

species. According to Wilcox (1955, p. 6), "Plants usually show no 

symptoms of boron deficiency if irrigated with water containing at 

least 0.1 ppm of boron, but injury may develop on the more sensitive 

plants when irrigated with water containing boron in excess of 1 ppm." 

According to the California Water Pollution Control Board (California Institute of Technology, 1957, p. 149), "It is doubtful whether 

more than 0.5 ppm can be applied continuously to soils without ultimately producing some plant injury.'' The concentrations of boron
H46 CONTRIBUTIONS TO THE HYDROLOGY OF THE UNITED STATES

in most of the water from sands and gravels of Pleistocene age and 

from alluvium are between 0.1 and 0.5 ppm, and the concentrations 

in most of the water from the Dakota group are more than 0.5 ppm.

High concentrations of bicarbonate in irrigation water may cause 

the pH of the soil to increase and may lead to the development of 

"black alkali" soil. As the water evaporates and the calcium and 

magnesium precipitate, any remaining bicarbonate combines with 

sodium to form sodium carbonate, which raises the pH of the soil. 

Wilcox, Blair, and Bower (1954) concluded that if concentrations of 

bicarbonate do not exceed those of calcium and magnesium by more 

than 1.25 epm, the water probably is safe for use. The concentrations 

of bicarbonate in most of the water in Salt Creek basin do not exceed 

those of calcium and magnesium by more than 1.25 epm.

SUMMARY

Suspended-sediment data obtained from 1951 to 1954 on Salt Creek 

at Lincoln, Nebr., indicate that 75 percent or more of the total annual 

suspended-sediment discharge is transported by flow that is exceeded 

5 percent or less of the time each year. Estimates from sediment 

data for 1951-54 and flow-duration data for 1950-59 indicate that the 

sediment discharge for the period 1950-59 was about 18.7 million tons.

Suspended-sediment concentrations varied widely. From March 

1951 to September 1954 the minimum measured concentration was 9 

ppm, and the maximum was 69,100 ppm.

Computations indicate that the measured sediment discharge is 

most of the total sediment discharge over a wide range of water and 

sediment discharges.

Water from most wells in the Dakota group contains high concentrations of dissolved solids and is of the sodium chloride type. Water 

from the sands and gravels of Pleistocene age in the southern half of 

the basin generally contains less than 1,000 ppm of dissolved solids, 

and water in the northern half generally contains less than 500 ppm. 

The water in the alluvium probably is of the calcium bicarbonate type 

and has less than 1,000 ppm of dissolved solids except where water of 

the sodium chloride type has infiltrated the alluvium.

During low discharge the water in the upstream parts of Salt Creek 

and its tributaries is similar in chemical quality to the water from sands 

and gravels of Pleistocene age, and water in the vicinity of Lincoln 

is similar in chemical quality to the water from the Dakota group.

Water from most public supplies contains less than 500 ppm of dissolved solids but is very hard; iron and manganese in many of the 

supplies exceeded recommended maximum concentrations. The water 

from the Dakota group is unsatisfactory for irrigation, and most of
SEDIMENTATION, QUALITY OF WATER, SALT CREEK, NEBR. H47

the water from the deposits of Pleistocene age and from the alluvium 

can be used for irrigation if drainage is adequate and if plants having 

good salt tolerance are grown.

SELECTED BIBLIOGRAPHY

American Water Works Association, 1950, Water quality and treatment, 2d

ed.: p. 54. 

Beesley, T. E., and others, 1948, Soil survey, Lancaster County, Nebraska: U.S.

Dept. Agriculture, ser. 1938, no. 15, 70 p. 

California Institute of Technology, 1957, Water quality criteria: State Water

Pollution Control Board pub. 3, 2d printing, 676 p. 

Colby, B. R., 1957, Relationship of unmeasured sediment discharge to mean

velocity: Am. Geophys. Union Trans., v. 38, no. 5, p. 708-717. 

Condra, G. E., and Reed, E. C., 1939, Deep wells at Lincoln, Nebraska: Nebraska

Geol. Survey Paper 15.

 1943," The geological section of Nebraska: Nebraska Geol. Survey Bull. 

14, 82 p.

 1950, Correlation of the Pleistocene deposits of Nebraska: Nebraska

Geol. Survey Bull. ISA, 74 p. 

Eaton, F.M., 1950, Significance of carbonates in irrigation waters: Soil Sci.,

v. 69, no. 2, p. 123-133.

Lane, E. W., and others, 1947, Report of the subcommittee on sediment terminology : Am. Geophys. Union Trans., v. 28, no. 6, p. 936-938. 

Leopold, L. B., and Wolman, M. G., 1957, River channel patterns braided,

meandering, and straight: U.S. Geol. Survey Prof. Paper 282-B, 47 p. 

Maxcy, K. F., 1950, Report on the relation of nitrate concentrations in well

waters to the occurrence of methemoglobinemia: Natl. Research Council

Bull., Sanitary Engineer, app. D, p. 265. 

Musgrave, G. W., 1957, Hydrologic soil groups, in Mockus, Victor, and others,

Hydrology: U.S. Dept. Agriculture, Eng. Handb., sec. 4, suppl. A, p. 3.7-1. 

Reed, E. C., 1951, Generalized geologic bedrock map of Salt Creek basin: Nebraska

Univ. Conserv. and Survey Div. 

Scofield, C. S., 1936, The salinity of irrigation water: Smithsonian Inst. Ann.

Rept., 1935, p. 275-287. 

Stiff, H. A., Jr., 1951, The interprentation of chemical water analysis by means

of patterns: Petroleum Tech. Jour., Tech. Note 84, sec. 1, p. 15-16. 

U.S. Public Health Service, 1961, Drinking water standards, 1961: Am. Water

Works Assoc. Jour., v. 53, no. 8, p. 935-945. 

U.S. Salinity Laboratory Staff, 1954, Diagnosis and improvement of saline and

alkali soils: U.S. Dept. Agriculture, Agriculture Handb. 60, 160 p. 

Welsh, G. B., and Thomas, J. F., 1960, Significance of chemical limits in USPHS

drinking water standards: Am. Water Works Assoc. Jour., v. 52, no. 3, p.

289-300.

Wilcox, L. V., 1948, The quality of water for irrigation use: U.S. Dept. Agriculture Tech. Bull. 962, 40 p.

 1955, Classification and use of irrigation waters: U.S. Dept. Agriculture 

Circ. 969, 19 p.

Wilcox, L. V., Blair, G. Y., and Bower, C. A., 1954, Effect of bicarbonate on suitability of water for irrigation: Soil Sci., v. 77, p. 259-266.

o