U.S. Department of the Interior

U.S. Geological Survey

Historical Channel Change Along

Soldier Creek, Northeast Kansas

By KYLE E. JURACEK

Water-Resources Investigations Report 02–4047

Prepared in cooperation with

PRAIRIE BAND POTAWATOMI NATION

Lawrence, Kansas

2002

U.S. Department of the Interior

U.S. Geological Survey

Cover photograph: Rocky Ford on Soldier Creek, northeast Kansas, October 24, 2001.
U.S. Department of the Interior

Gale A. Norton, Secretary

U.S. Geological Survey

Charles G. Groat, Director

For additional information write to: Copies of this report can be purchased fro

District Chief U.S. Geological Survey

U.S. Geological Survey Information Services

4821 Quail Crest Place Building 810

Lawrence, KS 66049–3839 Box 25286, Federal Center

Denver, CO 80225–0286
Content

CONTENTS

Abstract.................................................................................................................................................................................. 

Introduction ........................................................................................................................................................................... 

Description of Soldier Creek Basin ....................................................................................................................................... 

Methods ................................................................................................................................................................................. 

Historical Channel Change.................................................................................................................................................... 

Soldier Creek near Topeka........................................................................................................................................... 

Soldier Creek near Delia.............................................................................................................................................. 

Soldier Creek near Saint Clere .................................................................................................................................... 

Soldier Creek near Circleville ..................................................................................................................................... 

Soldier Creek near Soldier........................................................................................................................................... 

Soldier Creek near Bancroft ........................................................................................................................................ 

Soldier Creek near Goff............................................................................................................................................... 

Kansas River at Topeka ............................................................................................................................................... 

Discussion.............................................................................................................................................................................. 

Summary and Conclusions .................................................................................................................................................... 

References ............................................................................................................................................................................. 

FIGURES

1. Maps showing location of Soldier Creek Basin, Soldier Creek, major tributaries, Prairie Band Potawatomi

Nation Reservation, channelized section, weirs, and U.S. Geological Survey streamflow-gaging stations,

northeast Kansas...................................................................................................................................................... 

2. Map showing land use in Soldier Creek Basin, circa 1992..................................................................................... 

3–8. Graph showing:

3. Variation in stream stage for mean annual discharge at Soldier Creek gaging station near Topeka, 1936–99 . 

4. Relation between discharge and channel width at Soldier Creek gaging station near Topeka, pre- and

post-channelization............................................................................................................................................ 

5. Variation in stream stage for mean annual discharge at Soldier Creek gaging station near Delia, 1958–99 .... 

6. Relation between discharge and channel width at Soldier Creek gaging station near Delia............................. 

7. Relation between discharge and channel area at Soldier Creek gaging station near Delia ............................... 

8. Relation between discharge and streamflow velocity at Soldier Creek gaging station near Delia.................... 

9–13. Graph showing variation in stream stage for mean annual discharge at Soldier Creek gaging station near:

9. Saint Clere, 1964–78 ........................................................................................................................................ 

10. Circleville, 1964–97........................................................................................................................................... 

11. Soldier, 1964–95................................................................................................................................................ 

12. Bancroft, 1964–81 ............................................................................................................................................. 

13. Goff, 1964–80.................................................................................................................................................... 

14. Graph showing variation in river stage for mean annual discharge at Kansas River gaging station at Topeka,

1961–95................................................................................................................................................................... 

15. Map showing historical trends and rates of channel-bed elevation change at U.S. Geological Survey

streamflow-gaging stations located on Soldier Creek and Kansas River................................................................ 

TABLE

1. U.S. Geological Survey streamflow-gaging stations on Soldier Creek and Kansas River, northeast Kansas......... 
IV Historical Channel Change Along Soldier Creek, Northeast Kansas

CONVERSION FACTORS AND ABBREVIATIONS

Multiply By To obtain

cubic foot per second (ft3/s) 0.02832 cubic meter per second

foot (ft) 0.3048 meter

foot per second (ft/s) 0.3048 meter per second

foot per year (ft/yr) 0.3048 meter per year

inch (in.) 2.54 centimeter

inch per hour (in/hr) 2.54 centimeter per hour

mile (mi) 1.609 kilometer

mile per year (mi/yr) 1.609 kilometer per year

square foot (ft2) 0.09290 square meter

square mile (mi2) 640 acre

square mile (mi2) 259.0 hectare

square mile (mi2) 2.590 square kilometer
Introductio

Historical Channel Change Along Soldier Creek, Northeast

Kansas

By Kyle E. Juracek

Abstract

To assess historical channel change along

Soldier Creek, northeast Kansas, available

information from eight U.S. Geological Survey

streamflow-gaging stations was analyzed. At each

gaging station, channel change was assessed

using channel-bed elevation as the primary indicator variable. Changes in channel-bed elevation

were inferred from changes in the stage associated with the mean annual discharge at each

station. The variables channel width, channel

area, and streamflow velocity were used as

additional indicators of change.

Results indicated that the most substantial

channel changes occurred downstream from

Rocky Ford at the Soldier Creek streamflowgaging stations located near Topeka and Delia.

The available evidence indicated that the channelization of Soldier Creek, completed in 1961, was

likely the primary cause of the channel changes

at these locations. The decreasing base level

provided by the Kansas River also may have contributed to the channel changes at these locations. At the Soldier Creek gaging station near

Topeka, immediate effects of the channelization

included a decrease in channel-bed elevation of

about 5 feet and an increase in channel width of

about 35 feet. The instability introduced by the

channelization caused channel-bed degradation

that moved upstream at the rate of about 0.7 to

1.2 miles per year. At the Soldier Creek gaging

station near Delia, located about 12 miles

upstream from the upstream end of the channelized section, channel-bed degradation began during the 1970s and resulted in a net decrease in

channel-bed elevation of about 5 feet by 1999

The available evidence indicated that Sold

Creek at and upstream from Rocky Ford has n

been substantially affected by the upstreamprogressing channel-bed degradation as of 20

In this part of the basin other causes of chann

change, such as land use and floods, may be

relatively more important.

INTRODUCTION

 Soldier Creek is an important resource for the

Prairie Band Potawatomi Nation as it flows direct

through their reservation in Jackson County, Kans

(fig. 1). The habitat provided by the creek support

wildlife that helps meet the subsistence fishing an

hunting needs of tribal members who supplement 

income by using wildlife for food. Additionally, th

creek is valued for its natural beauty and for provi

a setting for cultural and recreational activities. O

site that is particularly valued by tribal members i

Rocky Ford (fig. 1, see photograph on report cove

where limestone bedrock in the channel creates a

waterfall during low-flow periods.

Channel changes affecting Soldier Creek may

threaten the benefits that have been traditionally

enjoyed by tribal members. An understanding of 

channel changes is needed to address several impo

tant issues being considered by the Prairie Band P

watomi Nation, including the protection and

restoration of aquatic and riparian habitat, the pro

tion of property and structures from flooding and

erosion hazards, the preservation of the natural be

of the landscape, and the use of streams for cultur

and recreational activities.
2 Historical Channel Change Along Soldier Creek, Northeast Kansas

95°50'

96°

39°30'

20'

39°10'

06889100 (near Goff)

06889100

(near Goff)

06889120 (near Bancroft)

06889160 (near Circleville)

06889180 (near Saint Clere)

06889200

(near Delia)

06889140

(near Soldier)

Soldier

Topeka

Mayetta

Circleville

Soldier

Soldier

Little

South

Branch

Soldier

Creek Crow

James

Creek

Creek

Creek

Creek

Cree

k

Indian

Halfday

Messhoss

Silver Lake Ditch

Creek

Creek

Creek

Creek

Rocky

Ford

(bedrock

outcrop)

Dutch

Walnut

Nemaha County

Jackson County

Boundary of Prairie 

Band Potawatomi 

Nation Reservation

Boundary of

Soldier Creek

Basin

Channelized section of Soldier Creek

U.S. Geological Survey streamflow-

 gaging station and number

New U.S. Geological Survey streamflow-

 gaging station and number

Weir —Number in parentheses is year 

 completed

Shawnee County

Soldier Creek Basin

Index map

EXPLANATION

(1987)

(1987) (1984) (1989)

(1988)

(1991)

(1991)

(1990)

(1990)

(1983, 1989)

(1989)

(1989)

0 1 2 3 4 5 KILOMETERS

0 1 2 3 4 5 MILES

Base map from U.S. Geological Survey digital data, 1:2,000,000, 1994

Albers Conic Equal-Area projection,

Standard parallels 29°30' and 45°30', central meridian 96°

Basin boundary from U.S. Department of Agriculture,

Natural Resources Conservation Service (1997)

06889170 (near Holton)

06889170

(near Holton)

IVER NSAS R

AK

06889500

(near Topeka) 06889000

(at Topeka)

Figure 1. Location of Soldier Creek Basin, Soldier Creek, major tributaries, Prairie Band Potawatomi Nation

Reservation, channelized section, weirs, and U.S. Geological Survey streamflow-gaging stations, northeast

Kansas.
Introductio

Channel changes may have both natural and

human causes. Natural events such as floods may

cause substantial channel change in a short period of

time. Human disturbances such as channelization and

land-use change introduce instability to which streams

adjust over longer time periods by such processes as

channel degradation [that is, erosion of the channel

bed and (or) banks] and channel aggradation (that is,

deposition of material). Channelization, which usually

involves the straightening, deepening, and shortening

of stream channels, the consequence of which is an

increase in channel slope and streamflow velocity, can

cause significant channel degradation that will move

upstream from the original site of disturbance. Landuse changes, such as the conversion of forest and

grassland to cropland, may result in increased runoff,

increased sediment production, and streambank

erosion. Additional causes of channel change include

other channel modifications (for example, low-water

crossings, weirs, bridge work, and bank stabilization),

changes in base level (that is, the elevation below

which erosion cannot occur), and climate change.

Previous studies have documented channel

changes mostly caused by channelization of Soldier

Creek in and upstream from the city of Topeka in

Shawnee County, Kansas (fig. 1) (Booker, Engineers,

Architects, Planners, [1986a?]; U.S. Army Corps of

Engineers, 1988). In the vicinity of Topeka, Soldier

Creek was channelized on at least two separate occasions. By 1933, the Northeast Drainage District of

Topeka had channelized the downstream reaches of

Soldier Creek in an effort to minimize flooding. As a

result, the affected channel was reduced in length by

about 27 percent (Booker, Engineers, Architects, Planners [1986a?]). Then, the U.S. Army Corps of Engineers (USCOE), as part of the Topeka, Kansas, flood

protection project, constructed the Soldier Creek

diversion unit between March 1957 and November

1961. This channelization project realigned several

miles of Soldier Creek, reducing the affected channel

an additional 20 percent in length (Booker, Engineers,

Architects, Planners, [1986a?]). Also, the Soldier

Creek confluence with the Kansas River was relocated

1.6 mi farther downstream (U.S. Army Corps of Engineers, 1988). The enlarged, straightened, and deepened section of Soldier Creek extends about 10 stream

mi upstream from its confluence with the Kansas

River.

Cross-sectional surveys completed by the USCOE

indicated substantial channel changes in the years

following the completion of the Soldier Creek div

sion unit in November 1961. Cross-sectional surv

completed by the USCOE in 1969 and 1972 indic

as much as 4 to 10 ft of channel-bed degradation 

occurred at locations in the upstream part of the c

nelized section of Soldier Creek. Downstream, th

surveys indicated several feet of channel-bed agg

tion had occurred. Also, in 1969 a widening of th

channel bottom from 40 ft (original 1961 constru

width) to as much as 90 ft was determined near th

upstream end of the channelized section. Photogr

metric analysis completed by the USCOE in 1984

indicated that additional channel-bed degradation 

channel widening had occurred in the upstream en

the channelized section (U.S. Army Corps of Eng

neers, 1988).

To limit further degradation of the Soldier Cr

channel bed and banks, the North Topeka Drainag

District constructed a series of eight weirs during 

1980s and early 1990s. Built of concrete rubble, r

and sometimes topped with concrete, the weirs ar

located between about 2.0 and 6.5 stream mi upstr

from the near Topeka streamflow-gaging station

(station 06889500, fig. 1). Also, at the same time,

three weirs were constructed in the Little Soldier

Creek channel within about 1.5 stream mi of its

confluence with Soldier Creek (Dale Sundberg, N

Topeka Drainage District, written commun., 2001

To provide an assessment of channel change a

Soldier Creek, a study was undertaken by the U.S

Geological Survey (USGS) in cooperation with th

Prairie Band Potawatomi Nation. Specific objecti

were to:

(1) Determine the type, magnitude, timing, and ra

channel change that has occurred at specific

locations;

(2) Determine whether any trends in channel chan

exist throughout the basin; and

(3) Infer possible causes of past channel changes 

the possibility of future channel changes

throughout the basin.

The purpose of this report is to present the re

of the USGS assessment of channel change along

Soldier Creek. From a national perspective, the re

presented enhance the understanding of the geom

phic (channel-changing) effects of human disturba

on small streams. Also, the methods used and res

obtained will provide guidance and perspective fo

similar assessments conducted throughout the Na
4 Historical Channel Change Along Soldier Creek, Northeast Kansas

DESCRIPTION OF SOLDIER CREEK BASIN

The Soldier Creek Basin is an area of about

334 mi2

 that drains parts of Shawnee, Jackson, and

Nemaha Counties in northeast Kansas (fig. 1). Soldier

Creek is a meandering stream with steep banks. The

principal tributary to Soldier Creek is Little Soldier

Creek. Lesser tributaries, in downstream-to-upstream

order, include Indian Creek, Halfday Creek, Silver

Lake Ditch, Messhoss Creek, Walnut Creek, Dutch

Creek, James Creek, South Branch Soldier Creek, and

Crow Creek (fig. 1).

The Soldier Creek Basin is located within the Dissected Till Plains Section of the Central Lowland

Province (Fenneman, 1946). The Dissected Till Plains

are characterized by dissected deposits of Pleistocene

glacial till that consist of silt, clay, sand, gravel, and

boulders overlying bedrock. Within the basin, the bedrock is mostly Pennsylvanian and Permian limestone

and shale that dips gently northwestward (U.S. Army

Corps of Engineers, 1974; Carswell, 1981). The flood

plains of Soldier and Little Soldier Creeks consist of

Pleistocene and Holocene alluvium (Walters, 1953;

Carswell, 1981). The alluvium, which ranges in thickness up to 65 ft, generally consists of clay in the upper

30 to 40 ft underlain by as much as 30 ft of silty sand

and gravel (U.S. Army Corps of Engineers, 1974).

Soils within the basin are classified typically as either

silt loam, clay loam, or silty clay loam. The land

surface is rolling with gentle to moderate slopes generally less than 10 percent (U.S. Department of Agriculture, Soil Conservation Service, 1970, 1979). Slope,

along with soil permeability and land use (discussed in

a following paragraph), are important factors that

affect storm runoff, which in turn affects streamflow

and sediment loads and thus the size and shape of the

channel.

Depth-weighted, mean soil permeability in the

Soldier Creek Basin ranges from 0 to 2.2 in/hr with a

mean of about 0.5 in/hr. In general, soil permeability is

less in the uplands (typically less than 0.7 in/hr) and

higher in the flood plains (typically between 1.0 and

1.3 in/hr) (Juracek, 2000).

Long-term mean annual precipitation in the Soldier Creek Basin is about 35 in. at Topeka (period of

record 1948–2000) and about 36 in. at Circleville

(period of record 1971–2000). Most of the annual precipitation is received during the growing season, April

through September (High Plains Regional Climate

Center, 2001).

Land use is predominantly agricultural w

land, cropland, and woodland accounting for a

30, and 6 percent of the basin, respectively. M

the cropland is concentrated in the flood plain

Soldier and Little Soldier Creeks. Urban land 

accounts for less than 1 percent of the basin (

(Kansas Applied Remote Sensing Program, 1

METHODS

A stable stream channel naturally meande

its valley over time while maintaining approx

the same cross-sectional shape (Leopold, 199

Therefore, changes in channel shape may be 

infer channel instability (Thornes, 1977; Sim

Li, 1982). In this assessment, channel-bed ele

channel width, channel area, and streamflow 

were used as indicator variables of channel in

and historical channel change along Soldier C

Changes in channel-bed elevation were inferr

changes in the stage associated with the mean 

discharge at each streamflow-gaging station.

This assessment of temporal and spatial c

change used available information from seven 

streamflow-gaging stations previously or pres

located on Soldier Creek. Also, information 

gaging station on the Kansas River was analy

evaluate possible external basin controls of ch

change on Soldier Creek (fig. 1, table 1). The 

stations provide historical, site-specific chann

streamflow information that also may indicate 

tions both upstream and downstream of the st

On the basis of this site-specific information, 

ences can be made about possible causes of p

channel changes and the possibility of future 

changes throughout the basin.

At any given time and location along a riv

stream, a relation exists between river/stream 

(that is, the height of the water in the channel 

given datum) and discharge (that is, streamflo

volume per unit time). These relations, quanti

rating curves, are updated as necessary to acc

date changes in channel shape, slope, and othe

that can affect the relation. Each rating curve 

sents a best-fit line through the measurement d

is, paired measurements of river/stream stage 

discharge). Discharge measurements at, and s

discharge rating curves for, the streamflow-ga

tions were made using standard USGS techni
Method

39°30'

Topeka

h

Nemaha Count

Jackson Count

ne

nty

Base map from U.S. Geological Survey digital data, 1:2,000,000, 1994

Albers Conic Equal-Area projection,

Standard parallels 29°30' and 45°30', central meridian 96°

Land use from Kansas Applied

Remote Sensing Program (1993)

Bound

Soldie

Basin

0 1 2 3 4 5 KILOMETERS

0 1 2 3 4 5 MILES

R NS KA

Figure 2. Land use in Soldier Creek Basin, circa 1992.
6 Historical Channel Change Along Soldier Creek, Northeast Kansas

(Buchanan and Somers, 1969; Kennedy, 1984) with a

typical accuracy of +5 percent (Kennedy, 1983).

By computing the stage that relates to a reference

discharge for each rating curve developed during the

period of record of a gaging station (and correcting to

a common datum, if necessary), trends in the elevation

of the channel bed can be inferred by plotting the

resulting time-series data. In this assessment, the

river/stream stage for the mean annual discharge

(rounded to the nearest 1 or 10 ft3

/s, as appropriate)

for the period of record was used as the reference

discharge (Chen and others, 1999). If the stage for the

reference discharge has a downward trend, it may be

inferred that the channel-bed elevation has declined

over time due to erosion. Conversely, if the stage for

the reference discharge has an upward trend, it may be

inferred that the channel-bed elevation has risen over

time due to aggradation. No trend indicates that the

channel bed has been essentially stable.

In addition to the magnitude and trend of channelbed elevation changes at each gaging station, information derived from the rating curves also was used to

assess the rate of channel-bed elevation changes

(rating-curve information is on file at the USG

in Lawrence, Kansas). For a given trend, the 

channel-bed elevation change was estimated a

difference in stage (corresponding to the refer

discharge) between the starting and ending da

define the trend divided by the length of time 

the two dates.

Changes in channel width, channel area, 

streamflow velocity were assessed through an 

of discharge-width, discharge-area, and disch

velocity relations over a range of in-channel s

flow conditions for successive periods of time 

cover the period of record for each gaging sta

(discharge, channel-width, channel-area, and 

flow-velocity information is on file at the USG

in Lawrence, Kansas).

A statistical test was used to determine th

cance of any observed trends in channel chan

this purpose, a nonparametric Spearman’s rho 

tion coefficient was computed. An advantage 

man’s rho is that, because it is based on ranks

more resistant to the effects of extreme high a

values than the more commonly used Pearson

correlation coefficient (Helsel and Hirsch, 19

Trends were considered to be significant if th

bility (two-sided p-value) of rejecting a corre

hypothesis (in this case, no trend) was less th

equal to 0.05.

HISTORICAL CHANNEL CHANGE

In the following sections, the results of th

ses to assess changes in channel conditions at 

the seven streamflow-gaging sites located on 

Creek, as well as one streamflow-gaging site 

on the Kansas River at Topeka, are presented

results presented include the type, magnitude

rate, and trend of channel changes at each site

Soldier Creek near Topeka

The Soldier Creek streamflow-gaging sta

Topeka (station 06889500, fig. 1, table 1) is l

within the channelized section of Soldier Cre

sequently, the Soldier Creek channel at this si

directly affected by the channelization. A com

of stream stages for the mean annual dischar

(160 ft3/s) (a substitute for measured channel

elevation) before and after USCOE channeliz

Table 1. U.S Geological Survey (USGS) streamflow-gaging stations

on Soldier Creek and Kansas River, northeast Kansas

[--, not applicable]

USGS

station

number

(fig. 1)

USGS station

name

Approximate

distance

upstream

from confluence with

Kansas

River

(miles)

Approximate

drainage

area

(square

miles)

Period of

record

analyzed

06889100 Soldier Creek

near Goff

72 2 1964–87

06889120 Soldier Creek

near Bancroft

69 10 1964–88

06889140 Soldier Creek

near Soldier

66 17 1964–98

06889160 Soldier Creek

near Circleville

55 49 1964–2001

06889180 Soldier Creek

near Saint

Clere

45 80 1964–81

06889200 Soldier Creek

near Delia

22 157 1958–2001

06889500 Soldier Creek

near Topeka

6 290 1936–2001

06889000 Kansas River at

Topeka

-- -- 1961–2001
Historical Channel Chang

Stream stage, in feet

19301940195019601970198019902000

0

1

2

3

4

5

6

7

8

9

10

Channelization completed (1961)

Soldier Creek (1957–61) shows that there was about a

5-ft decline in channel-bed elevation at the time of the

channelization (fig. 3). Prior to channelization

between 1936 and 1956, the stream stage for the mean

annual discharge generally varied within + 1 ft of the

mean value of 8.2 ft, with a standard deviation of

about 0.5 ft. A statistically significant trend in stream

stage was not indicated for this time period (Spearman’s rho = -0.40, two-sided p-value = 0.08398).

Instead, the channel bed at this location appeared to

be fluctuating in response to scour (erosion) and fill

(deposition) processes that may reflect short-term

changes in response to individual flow events (fig. 3).

In figure 3 and subsequent figures that show changes

in the stage for the mean annual discharge over time,

each data point represents the stage for the mean

annual discharge on the date for which that specific

rating curve became effective.

Following completion of the channelization

project and the immediate lowering of the channel

elevation by about 5 ft, a steady decline in the stre

stage for the mean annual discharge (from about 3

to about 2 ft) was evident from 1962 to 1999 (fig. 

For this time period, a statistically significant

negative trend (that is, decreasing stream stage wi

time) (Spearman’s rho = -0.95, two-sided

p-value = 0.00000) was indicated. Since the

initial 5-ft decrease in elevation, the channel bed

continued to degrade from 1962 to 1999 at an ave

rate of about 0.03 ft/yr.

Channel width at the Soldier Creek gaging sta

near Topeka also changed substantially as an imm

ate result of the channelization. As shown in figur

post-channelization (1962–99) widths were gener

about 35 ft greater than pre-channelization

(1936–56) widths.

Figure 3. Variation in stream stage for mean annual discharge (160 ft3/s) at Soldier Creek gaging station near Topeka (station 06889

fig. 1), 1936–99.
8 Historical Channel Change Along Soldier Creek, Northeast Kansas

The analysis of relations between discharge and

channel area and between discharge and streamflow

velocity indicated that neither relation changed in

response to the channelization. For a given discharge,

the expected post-channelization response to

shortened channel length and increased slope would

be an increase in streamflow velocity and a decrease in

channel area. However, because the channelization

also included a widening of the channel bottom, the

changes in velocity and area did not occur. This is

because, with a wider channel, more of the streamflow

is closer to the channel perimeter where the velocity is

reduced by friction. Also, streamflow velocity at this

location occasionally may be reduced due to the

effects of backwater from the Kansas River.

Soldier Creek near Delia

The Soldier Creek streamflow-gaging sta

Delia (station 06889200, fig. 1, table 1) is loc

about 12 stream mi upstream from the upstrea

the channelized section of Soldier Creek and 

16 stream mi upstream from the near Topeka 

station (06889500, fig. 1). This gaging-statio

also located about 6.5 stream mi downstream 

southern boundary of the Prairie Band Potaw

Nation Reservation (hereafter referred to as th

vation). Available information indicated that t

channel at this location was straightened in co

tion with bridge construction in the mid-1950

Kennedy, U.S. Geological Survey, written com

Figure 4. Relation between discharge and channel width at Soldier Creek gaging station near Topeka

(station 06889500, fig. 1), pre- and post-channelization.

Discharge, in cubic feet per second

Channel width, in feet

0 250 500 750 1,000 1,250 1,500 1,750 2,000 2,250 2,500 2,750 3,000

30

40

50

60

70

80

90

100

110

120

130

Pre-channelization, 1936–56

Post-channelization, 1962–99
Historical Channel Chang

195019601970198019902000

5

6

7

8

9

10

11

12

13

14

15

Stream stage, in feet

Low-water crossing

completed (1971)

Low-water crossing

partially washed out

(1978)

1958). A channel cutoff occurred about 0.25 mi

downstream from the gaging station some time

between 1967 and 1977 (U.S. Army Corps of Engineers, 1988), with a resultant shortening of the

channel length by about 1,100 ft. On January 9, 1971,

a low-water crossing for heavy equipment was constructed with large rock about 1,500 ft downstream

from the gaging station (G.G. Quy, U.S. Geological

Survey, written commun., 1972). The low-water crossing was partially washed out in 1978.

Three distinct periods of channel-bed activity

were apparent for the period 1958 to 1999 (fig. 5). For

1958–70, the stream stage for the mean annual discharge (100 ft3

/s) varied about the mean value of

11.0 ft with a standard deviation of about 0.5 ft (fig. 5).

A statistically significant trend in stream stage was not

indicated for this time period (Spearman’s rho = 0.28,

two-sided p-value = 0.23406). Instead, the channel bed

at this location appeared to be fluctuating in response

to scour and fill processes in a manner similar to the

pre-channelization channel-bed activity at the nea

Topeka gaging-station site (fig. 3). Of note during 

period were large bank collapses that occurred fo

ing high flows on at least two occasions during 19

(K.L. Lindskov, U.S. Geological Survey, written c

mun., 1966). The bank collapses may have been

caused, in part, by the artificial straightening of th

channel at the Soldier Creek near Delia gaging sta

site about a decade earlier.

For 1971–78, the stream stage for the mean an

discharge increased from 12.4 to 13.9 ft (fig. 5). T

indicated an increase in the channel-bed elevation 

1.5 ft. For this time period, a statistically significa

positive trend was indicated (Spearman's rho = 0.

two-sided p-value = 0.00000). During this time pe

the channel bed aggraded at an average rate of ab

0.2 ft/yr.

For 1978–99, the stream stage for the mean an

discharge decreased from 13.9 to 7.3 ft (fig. 5). T

indicated a decrease in the channel-bed elevation 

Figure 5. Variation in stream stage for mean annual discharge (100 ft3/s) at Soldier Creek gaging station near Delia (station 06889

fig. 1), 1958–99.
10 Historical Channel Change Along Soldier Creek, Northeast Kansas

6.6 ft. For this time period, a statistically significant

negative trend was indicated (Spearman’s rho = -1.00,

two-sided p-value = 0.00000). During this time period,

the channel bed degraded at an average rate of about

0.3 ft/yr. The slope of the data points in figure 5

indicates that, as of 1999, the rate of channel-bed degradation had not yet begun to slow. Thus, unless bedrock is encountered or grade-control structures are

built, additional channel-bed degradation at the Delia

gaging-station site is likely.

Analysis of the relations between discharge and

channel width, channel area, and streamflow velocity

indicated a change in all three relations that appeared

to correspond with the channel-bed degradation that

began in the late 1970s. As shown in figure 6, the relation between discharge and channel width was similar

for the period 1958–99 for discharges less tha

about 750 ft3

/s. However, for discharges large

750 ft3

/s, the associated channel widths were 

for 1978–99 than for 1958–77. The difference 

most pronounced for discharges larger than a

1,250 ft3

/s for which channel widths were gen

about 70 ft less for 1978–99 (fig. 6). The decr

channel widths for the larger discharges was in

of a channel that has entrenched (that is, dow

The pattern of change for the relation bet

discharge and channel area was similar. As sh

figure 7, the relation between discharge and c

area was consistent for the period 1958–99 fo

charges less than about 1,000 ft3

/s. For discha

larger than 1,000 ft3

/s, the associated channel 

were generally smaller for 1978–99 than for 1

Figure 6. Relation between discharge and channel width at Soldier Creek gaging station near Delia

(station 06889200, fig. 1).

Discharge, in cubic feet per second

0 250 500 750 1,000 1,250 1,500 1,750 2,000 2,250 2,500 2,750 3,000

0

20

40

60

80

100

120

140

160

180

200

Channel width, in feet

1958–77

1978–99
Historical Channel Change 

Discharge, in cubic feet per second

0 250 500 750 1,000 1,250 1,500 1,750 2,000 2,250 2,500 2,750 3,000

0

200

400

600

800

1,000

1,200

1,400

1,600

1,800

Channel area, in square feet

1958–77

1978–99

The difference was more pronounced for the larger

discharges (fig. 7).

The relation between discharge and streamflow

velocity exhibited considerable scatter, which in part

may be attributed to problems associated with debris

and beaver dams in the vicinity of the gaging-station

site near Delia. For 1958–67 (data not shown), there

was no discernible relation between discharge and

velocity. For 1968–99, shown in figure 8, the expected

pattern of increasing velocity with increasing discharge was apparent. Despite the scatter, a pattern of

increased velocity over time was indicated. Possible

explanations for the increased velocity, and associated

decreased channel areas, are an increase in channel

slope and (or) a decrease in channel roughness.

Soldier Creek near Saint Clere

The streamflow-gaging station for Soldier Cr

near Saint Clere (station 06889180, fig. 1, table 1

located within the reservation about 23 stream mi

upstream from the Delia gaging station (station

number 06889200, fig. 1) and about 16 stream mi

upstream from Rocky Ford (which is just upstream

from the southern reservation boundary). Unfortu

nately, this gaging station was only active from 19

to 1981. In 1981, the bridge at this site was remov

and replaced with a low-water crossing. Thus, the

gaging station was discontinued. In 1985, the pre

(2001) bridge was constructed.

Figure 7. Relation between discharge and channel area at Soldier Creek gaging station near Delia

(station 06889200, fig. 1).
12 Historical Channel Change Along Soldier Creek, Northeast Kansas

Discharge, in cubic feet per second

0 250 500 750 1,000 1,250 1,500 1,750 2,000 2,250 2,500 2,750 3,000

0

0.5

1.0

1.5

2.0

2.5

3.0

3.5

4.0

Streamflow velocity, in feet per second

1968–77

1978–88

1993–99

For 1964–78, the stream stage for the mean annual

discharge (50 ft3

/s) showed minimal change (fig. 9).

Stream stage varied closely about the mean of 4.0 ft

with a standard deviation of about 0.2 ft. A statistically

significant positive trend (that is, increasing stage

with time) (Spearman’s rho = 0.50, two-sided

p-value = 0.00904) was indicated. However,

inspection of figure 9 shows that the aggradation that

occurred was minor. From 1978 to 1981, the channel

bed was apparently stable (as evidenced by the fact

that no new rating curves were developed during this

time period). No obvious changes in the relations

between discharge and channel width, channel area,

and streamflow velocity were indicated for this site.

Soldier Creek near Circleville

The streamflow-gaging station for Soldie

near Circleville (station 06889160, fig. 1, tabl

located about 10 stream mi upstream from the 

Clere gaging-station site (station 06889180, fi

about 5 stream mi upstream from the northern

boundary of the reservation. The Circleville g

station was discontinued in 2001 due to the p

replacement of the bridge. In its place, a new 

Creek near Holton” station (06889170) was e

lished about 3 stream mi downstream (fig. 1). 

gaging station is located about 2 stream mi up

from the northern boundary of the reservation

Figure 8. Relation between discharge and streamflow velocity at Soldier Creek gaging station near Delia

(station 06889200, fig. 1).
Historical Channel Change 

1960 1965 1970 1975 1980 

0

1

2

3

4

5

6

7

8

Stream stage, in feet

Three distinct periods of channel-bed activity

were apparent for the period 1964 to 1997 (fig. 10).

For 1964–72, the stream stage for the mean annual discharge (30 ft3

/s) varied about the mean value of 3.7 ft

with a standard deviation of about 0.2 ft. A statistically

significant trend in stream stage was not indicated for

this time period (Spearman's rho = 0.37, two-sided

p-value = 0.12831). Instead, the channel bed at this

location appeared to be fluctuating in response to

scour and fill processes (fig. 10).

 For 1972–92, the stream stage for the mean

annual discharge decreased from 3.9 to 2.45 ft

(fig. 10). This indicated a decrease in the channel-bed

elevation of 1.45 ft. For this time period, a statistically

significant negative trend was indicated (Spearman's

rho = -0.95, two-sided p-value = 0.00000). During this

time period, the channel bed degraded at an average

rate of about 0.07 ft/yr. For 1992–97, the channel bed

was relatively stable. Likewise, the channel bed was

apparently stable from 1997 to 2000 (as indicated 

the fact that no new rating curves were developed

during this time period).

The analysis of the relations between dischar

and channel width and between discharge and cha

area indicated that neither relation changed appre

bly during the period of record. The relation betw

discharge and streamflow velocity was not discern

and was characterized by considerable scatter. Th

lack of a relation between discharge and streamflo

velocity was due, in part, to problems associated 

debris and beaver dams in the vicinity of the gagi

station.

Soldier Creek near Soldier

The streamflow-gaging station for Soldier Cr

near Soldier (station 06889140, fig. 1, table 1) is

located about 11 stream mi upstream from the Cir

Figure 9. Variation in stream stage for mean annual discharge (50 ft3/s) at Soldier Creek gaging station near Saint Clere (station 068

fig. 1), 1964–78.
14 Historical Channel Change Along Soldier Creek, Northeast Kansas 1960 1965 1970 1975

1980198519901995

0

1

2

3

4

5

6

7

Stream stage, in feet

ville gaging-station site (station 06889160, fig. 1).

For 1964–95, a statistically significant negative

trend (Spearman’s rho = -0.87, two-sided

p-value = 0.00000) in stream stage for the mean

annual discharge (10 ft3

/s) was indicated (fig. 11).

During this time period, the stream stage for the mean

annual discharge decreased from 2.95 to 1.10 ft, which

indicated a decrease in channel-bed elevation of

1.85 ft. The average rate of channel-bed decline

during this period was about 0.06 ft/yr. However, the

degradation was not uniform over time. The most

pronounced degradation at this gaging-station site

occurred in the 1960s. From 1964 to 1969, the stream

stage for the mean annual discharge decreased 1.2 ft at

an average rate of about 0.2 ft/yr. Then, following the

deposition and subsequent erosion of 1.2 ft of sediment, the degradation continued during the period

1973–86 at an average rate of about 0.05 ft/yr. For

1986–95, the channel bed was relatively stable

(fig. 11). Likewise, the channel bed was appa

stable from 1995 to 1998 (as indicated by the 

no new rating curves were developed during t

period).

No discernible changes in the relations be

discharge and channel width, channel area, an

streamflow velocity were indicated for this ga

station site. The relation between discharge a

streamflow velocity exhibited some scatter, w

caused, in part, by problems with debris and b

dams in the vicinity of the gaging station.

Soldier Creek near Bancroft

The streamflow-gaging station for Soldie

near Bancroft (station 06889120, fig. 1, table 

located about 3 stream mi upstream from the 

gaging-station site (station 06889140, fig. 1).

For 1964–81, a statistically significant negativ

Figure 10. Variation in stream stage for mean annual discharge (30 ft3/s) at Soldier Creek gaging station near Circleville

(station 06889160, fig. 1), 1964–97.
Historical Channel Change 

19601965197019751980198519901995

0

1

2

3

4

5

Stream stage, in feet

trend (Spearman’s rho = -0.82, two-sided

p-value = 0.00000) was indicated for the change in

stream stage for the mean annual discharge (7 ft3/s)

(fig. 12). From 1964 to 1977, the stream stage for the

mean annual discharge decreased from 3.45 to 2.70 ft.

This indicated a decrease in the channel-bed elevation

of 0.75 ft at an average rate of about 0.06 ft/yr. The

overall trend of degradation during this time period

was characterized by several periods of scour and fill.

From 1977 to 1981, the channel bed was apparently

stable (fig. 12). The channel bed also was apparently

stable from 1982 to 1988 (as indicated by the fact that

no new rating curves were developed during this time

period). Due to limited information and artificial control provided by concrete bridge abutments, an assessment of changes in the relations between discharge

and channel width, channel area, and streamflow

velocity for the period of record was not possible 

this gaging-station site.

Soldier Creek near Goff

The streamflow-gaging station for Soldier Cr

near Goff (station 06889100, fig. 1, table 1) is loc

about 3 stream mi upstream from the Bancroft ga

station site (station 06889120, fig. 1) and is the m

upstream station on Soldier Creek. With one exc

tion, the channel bed at this location has been rela

tively stable. For 1964–69, the stream stage for th

mean annual discharge (1 ft3

/s) varied about the m

value of 2.2 ft with a standard deviation of about 0

A statistically significant trend in stream stage wa

indicated for this time period (Spearman's rho = 0

two-sided p-value = 0.58252). Instead, the channe

Figure 11. Variation in stream stage for mean annual discharge (10 ft3/s) at Soldier Creek gaging station near Soldier (station 06889

fig. 1), 1964–95.
16 Historical Channel Change Along Soldier Creek, Northeast Kansas

1960 1965 1970 1975 1980 1985 

0

1

2

3

4

5

6

Stream stage, in feet

at this location appeared to be fluctuating in response

to scour and fill processes (fig. 13).

The exception occurred from 1970 to 1973 when

about 1 ft of sediment was deposited and then partially

eroded. The channel bed appeared to stabilize during

the period 1974–80 with the stream stage for the mean

annual discharge averaging about 3 ft. The channel

bed also was apparently stable from 1980 to 1987 (as

indicated by the fact that no new rating curves were

developed during this time period). Due to limited

information, an assessment of changes in the relations

between discharge and channel width, channel area,

and streamflow velocity for the period of record was

not possible for this site.

Kansas River at Topeka

The Kansas River streamflow-gaging station at

Topeka (station 06889000, fig. 1, table 1) is located

about 2.3 river mi upstream from the Soldier 

confluence. For 1961–95, the river stage for t

annual discharge (6,000 ft3

/s) decreased from 

8.35 ft (fig. 14). This indicated a decrease in 

channel-bed elevation of 2.25 ft at an average 

rate of about 0.07 ft/yr. For this time period, a

statistically significant negative trend (Spearm

rho = -0.95, two-sided p-value = 0.00000) wa

cated. The channel bed was apparently stable 

1995 to 2000 (as indicated by the fact that no 

ing curves were developed during this time pe

Changes in channel width, channel area, and 

flow velocity were not assessed for this site.

DISCUSSION

Channel change may result from a variety 

human and natural causes. Human causes inc

channel modifications such as channelization

Figure 12. Variation in stream stage for mean annual discharge (7 ft3/s) at Soldier Creek gaging station near Bancroft (station 

fig. 1), 1964–81.
Discussion 

1960 1965 1970 1975 1980 1985 19

0

1

2

3

4

5

6

Stream stage, in feet

water crossings, weirs, bridge work, and bank stabilization, as well as land-use change. Natural causes,

which also may be affected by human activity, include

base-level change, floods, and climate change. As

evidenced by the spatial and temporal variability of

channel changes throughout the basin (fig. 15), many

of these causes may have contributed to channel

changes along Soldier Creek. In the following paragraphs, these potential causes of channel change are

discussed within the context of the analysis of data

from USGS streamflow-gaging stations located in or

near the Soldier Creek Basin.

Channel degradation represents the expected

response of Soldier Creek as it adjusts to the changes

introduced by channelization in an attempt to establish

a new equilibrium condition (Knighton, 1998). As the

adjustment progresses, channel degradation will move

upstream from the original site of channelization and

affect additional reaches of Soldier Creek as well as its

tributaries. The magnitude and extent of the upstream

channel degradation has not been determined. However, it has been proposed that channel-bed degradation of 4 to 9 ft, with accompanying bank erosion, may

be expected along Soldier Creek in Shawnee County

(upstream from Topeka) during the next few deca

(Booker, Engineers, Architects, Planners, [1986b

The susceptibility of a channel to upstreamprogressing degradation is controlled by a numbe

factors, including discharge, sediment load, bed a

bank material composition, local bed-elevation co

(for example, bedrock, armoring), and vegetation

Also, human-caused changes such as grade-contr

structures (for example, low-water crossings, wei

and bank stabilization may affect the response of 

stream channel. Considerable variation in the typ

magnitude, and rate of channel degradation may o

even between sites located close together due to t

variability of the controlling factors. If unchecked 

natural and (or) human-caused factors, the upstre

progressing degradation potentially may affect th

stream network throughout the entire basin.

Since completion of the USCOE channelizati

project in 1961, channel-bed degradation has migr

upstream to the streamflow-gaging station near D

(station 06889200, fig. 15). The gaging station ne

Delia is located about 12 stream mi upstream from 

upstream end of the channelized section of Soldie

Creek.

Figure 13. Variation in stream stage for mean annual discharge (1 ft3/s) at Soldier Creek gaging station near Goff (station 068891

fig. 1), 1964–80.
18 Historical Channel Change Along Soldier Creek, Northeast Kansas 1960 1965 1970 1975

1980198519901995

5

6

7

8

9

10

11

12

13

14

River stage, in feet

As of January 1971, when a low-water crossing

was constructed about 1,500 ft downstream from the

Delia gaging station, the upstream progression of

channel-bed degradation had not yet reached the

gaging station near Delia (figs. 5 and 15). Subsequently, when the low-water crossing partially washed

out in 1978, channel-bed degradation began and

continued at least through 1999. The correspondence

of the beginning of channel-bed degradation with the

partial washout of the low-water crossing indicated

that the low-water crossing temporarily may have

prevented the upstream progression of channel-bed

degradation that would have reached the gaging

station as early as 1971 or as late as 1978. This translates to a total traveltime of 10 to 17 years for the

degradation to migrate from the upstream end of the

channelized section of Soldier Creek to the gaging

station near Delia (fig. 15). Using the upstream end of

the channelized section as the point of reference, the

average rate at which the channel-bed degrad

progressed the 12 stream mi upstream to reac

Delia gaging-station site was 0.7 to 1.2 mi/yr

An additional factor that may have contri

channel-bed degradation at the Delia gaging s

was a channel cutoff that occurred about 0.25 

downstream some time between 1967 and 19

resultant shortening of the channel locally inc

the channel slope and streamflow velocity and 

erosive capability of the stream. With continu

nel-bed degradation at the Delia gaging-statio

is possible that a critical bank height eventual

be reached that causes the banks to become u

Such instability may initiate a period of bank 

and channel widening (Simon, 1989).

If uninhibited by bedrock or human-built

control structures, the post-1978 upstream pro

of channel-bed degradation (at the estimated 

0.7 to 1.2 mi/yr) potentially reached the south

Figure 14. Variation in river stage for mean annual discharge (6,000 ft3/s) at Kansas River gaging station at Topeka (station 06

fig. 1), 1961–95.
Discussion 

95°50'

96°

39°30'

20'

39°10'

06889100 (near Goff)

06889100

(near Goff)

06889120 (near Bancroft)

06889160 (near Circleville)

06889180 (near Saint Clere)

06889200

(near Delia)

06889140

(near Soldier)

Soldier

Topeka

Mayetta

Soldier

Soldier

Little

South

Branch

Soldier

Creek Crow

James

Creek

Creek

Creek

Creek

Creek

Indian

Halfday

Messhoss

Silver Lake Ditch

Creek

Creek

Creek

Creek

Rocky

Ford

(bedrock

outcrop)

Dutch

Walnut

Nemaha County

Jackson County

Boundary of Prairie 

Band Potawatomi 

Nation Reservation

Boundary of

Soldier Creek

Basin

Channelized section of Soldier Creek

U.S. Geological Survey streamflow-

 gaging station and number

New U.S. Geological Survey streamflow-

 gaging station and number

Weir —Number in parentheses is year 

 completed

No trend

Decreasing trend —Number is rate of decrease

 in feet per year

Increasing trend —Number is rate of increase,

 in feet per year

Shawnee County

EXPLANATION

(1987)

(1987) (1984) (1989)

(1988)

(1991)

(1991)

(1990)

(1990)

(1983,89)

(1989)

(1989)

0 1 2 3 4 5 KILOMETERS

0 1 2 3 4 5 MILES

Base map from U.S. Geological Survey digital data, 1:2,000,000, 1994

Albers Conic Equal-Area projection,

Standard parallels 29°30' and 45°30', central meridian 96°

Basin boundary from U.S. Department of Agriculture,

Natural Resources Conservation Service (1997)

06889170 (near Holton)

06889170

(near Holton)

IVER NSAS R

AK

06889500

(near Topeka) 06889000

(at Topeka)

1964 1969 1974 1987 Deposition and erosion of flood deposit, 1970–73 Trend in stage

1964 1977 1988

0.06

0.06

Trend in stage

1964 1969 1973 1986 1998 Deposition and erosion of flood deposit, 1970–73

0.2 0.05

Trend in stage

1964 1972 1992 2000

0.07

Trend in stage

1958 1970 1978 1999

0.2 0.3

Trend in stage

1936 1956 1962 1999

0.03

Trend in stage

1964 1978 1981

0.004

0.004

Trend in stage

1961 1995 

0.07

Trend in stage Channelization, 1957–61

Time perio

Time period

Time period

Time period

Time period

Time period

Time period

Time period

Figure 15. Historical trends and rates of channel-bed elevation change at U.S. Geological Survey streamflow-gaging stations loc

on Soldier Creek and Kansas River.
20 Historical Channel Change Along Soldier Creek, Northeast Kansas

boundary of the reservation, located about 6.5 stream

mi upstream from the Delia gaging station, in about

5 to 9 years. Thus, the Soldier Creek channel bed at

this location potentially would have started to degrade

some time between 1983 and 1987.

For 1978–99, the channel bed at the Delia gaging

station decreased 6.6 ft at an average rate of about

0.3 ft/yr. However, if the 1.5 ft of aggradation apparently due to the presence of the low-water crossing is

discounted, the channel bed at this location decreased

5.1 ft at an average rate of about 0.2 ft/yr. Using the

average degradation rate determined for the Delia

gaging station (that is, 0.2 or 0.3 ft/yr), the channel

bed at the southern boundary of the reservation potentially degraded from 2.6 to 5.1 ft through 2000.

At Rocky Ford, located about 0.3 mi upstream

from the southern boundary of the reservation

(fig. 15), the upstream progression of channel-bed

degradation potentially arrived shortly after it crossed

the reservation boundary. Thus, potential channel-bed

degradation immediately downstream from Rocky

Ford is comparable to that which may have occurred at

the southern reservation boundary. Such degradation,

if it is occurring, may accelerate the undercutting and

eventual collapse of the bedrock that creates the lowflow waterfall at Rocky Ford. Evidence of channel-bed

degradation at Rocky Ford would include an increase

in the height of the waterfall.

In April 2001, the height of the waterfall at Rocky

Ford (measured from the top of the bedrock to the

downstream water surface during low-flow conditions)

was determined to be about 1.55 ft. Available evidence, which included an interview with a long-time

local resident and old photographs, indicated that the

height of the waterfall (during low-flow conditions) at

Rocky Ford has been about the same at least since the

1960s. Thus, as of April 2001, the channel bed immediately downstream from Rocky Ford apparently has

yet to be affected discernibly by the upstream progression of degradation.

Several possibilities may account for the apparent

lack of channel-bed degradation immediately downstream from Rocky Ford. For example, the upstream

progression of degradation may be inhibited by gradecontrol structures (for example, low-water crossings,

weirs). Onsite inspection of the Soldier Creek channel

between Rocky Ford and the Delia gaging-station

site determined that no such structures presently

(May 2001) exist. However, at one site, possible

evidence of a washed-out structure (large rocks and

concrete rubble in the channel) was found. Al

rocks were observed in the channel at two oth

sites—near a bridge and at a site where an att

bank stabilization had partially failed. Such ar

introduced rock may provide at least some tem

resistance to channel-bed degradation.

Another possibility is that natural channe

tions may have slowed or prevented the upstr

progression of degradation. Onsite inspection 

Soldier Creek channel between Rocky Ford a

Delia gaging-station site revealed that, at one 

where the channel is located next to an outcro

limestone and shale bedrock on the valley wa

deposit of loose bedrock debris had accumula

across the channel bed. The bedrock debris cr

rapid during low-flow conditions over which t

surface drops an estimated 1.5 ft. The loose b

debris at this site may provide at least some te

resistance to channel-bed degradation. Also, e

bedrock was observed across the channel bed 

located about 0.3 mi upstream from the Delia 

station site. Available evidence, which includ

interview with a long-time local resident and 

tion of exposed tree roots, indicated substanti

nel-bed erosion upstream from the bedrock o

Thus, the bedrock outcrop may have been exp

relatively recently. The bedrock may provide

resistance to future upstream progression of c

bed degradation.

Also, it is possible that the channel imme

downstream from Rocky Ford may be armore

armored channel bed is one in which the fine 

has been eroded and carried away leaving a la

coarse material that inhibits further degradati

channel bed. The armor on the channel bed at 

location may include cobble-sized material as 

bedrock slabs.

A final possibility is that a combination o

and human-caused conditions may have limit

upstream progression of channel-bed degrada

However, it is not known if the limitation is c

or partial, permanent or temporary. It is possi

with more time channel-bed degradation imm

downstream from Rocky Ford may become m

evident. The bedrock outcrop in the channel a

Ford should minimize the progression rate of 

bed degradation upstream from that site.

The weirs constructed upstream from the 

Creek near Topeka gaging station (06889500

by the North Topeka Drainage District, in the 
Summary and Conclusions 

and early 1990s, may prevent additional channel-bed

degradation from progressing upstream from those

structures. However, the substantial channel-bed degradation that occurred during the 1960s through the

early 1980s had already progressed upstream before

the weirs were built.

Bridge work may have contributed to channel

change at the Soldier Creek near Soldier streamflowgaging station (06889140, fig. 15). At this site, the

relatively rapid channel-bed degradation from 1964 to

1969 (compared to subsequent years) (fig. 11) may

have been caused, in part, by the disturbance of the

channel when the bridge was constructed not too long

before the gaging station was established (L.M. Pope,

U.S. Geological Survey, written commun., 1975).

The effects of land-use and climate changes on the

Soldier Creek channel cannot be determined solely on

the basis of the gaging-station information used in this

assessment. However, it is reasonable to expect that

land use and climate may have contributed to the channel-bed changes that occurred along Soldier Creek. In

particular, land-use and climate changes may be relatively more important as causes of channel change in

the upstream part of the Soldier Creek Basin

(upstream from Rocky Ford) (fig. 15), which does

not appear to have been affected by the downstream

channelization.

Base level is another factor that may contribute

to, or prevent, changes in channel-bed elevation. For

Soldier Creek, base level is provided by the Kansas

River. For 1961–95, the channel-bed elevation for the

Kansas River at Topeka streamflow-gaging station

(06889000, figs. 14 and 15) decreased 2.25 ft at an

average rate of 0.07 ft/yr. This decrease in base level

may have contributed to channel-bed degradation

along Soldier Creek downstream from Rocky Ford

(fig. 15). At Rocky Ford, the limestone bedrock in the

channel provides a local base-level control that will

minimize the rate of channel-bed degradation. Likewise, upstream at the Soldier Creek near Soldier

gaging station (06889140, fig. 15), base-level control

is provided by exposed bedrock that forms the channel

bed. Thus, unless disturbed by human activity, additional channel-bed degradation at this location also is

expected to be minimal.

Floods can cause substantial channel change in a

short period of time. Flood-related changes in channel-bed elevation were determined for two locations in

the upstream part of the basin. At the Soldier Creek

near Goff streamflow-gaging station (06889100,

figs. 13 and 15), two successive increases in chan

bed elevation (totaling about 1 ft) during 1970 we

apparently due to deposition of sediment caused b

high flows on May 10 and May 23, 1970. The Ma

flood was the largest for the period of record (peak 

charge of 7,080 ft3

/s). Downstream at the Soldier

Creek near Soldier gaging station (06889140, figs

and 15), a degradational trend was interrupted on

May 10, 1970, when the largest flood for the perio

record (peak discharge of 11,700 ft3/s) deposited 

of sediment in the channel. Unlike the Goff (upstre

and Soldier (downstream) gaging-station sites, th

Soldier Creek near Bancroft gaging station (06889

figs. 12 and 15) did not have a substantial deposit

of sediment caused by the May 10, 1970 flood, w

was the largest for the period of record at this site

(peak discharge of 13,100 ft3

/s). In addition, the

May 10, 1970 flood apparently had little effect on

channel-bed elevation at other downstream gagin

stations. By the time the flood reached the gaging

station near Circleville, its peak discharge had dim

ished to 5,570 ft3

/s.

SUMMARY AND CONCLUSIONS

Available information from eight U.S. Geolog

Survey streamflow-gaging stations was used to as

historical channel change along Soldier Creek, no

east Kansas. For each gaging station, channel cha

was assessed using channel-bed elevation as the

primary indicator variable. Changes in channel-b

elevation were inferred from changes in the stage

associated with the mean annual discharge at each

station. The variables channel width, channel area

streamflow velocity were used as additional indic

of change.

Results indicated that the most substantial cha

changes in the basin occurred downstream from R

Ford at the Soldier Creek streamflow-gaging stati

located near Topeka and Delia. The available evi

dence indicated that channelization was likely the

primary cause of the channel changes at these loc

tions. The channel-bed degradation at these locat

also may have been caused, in part, by the decrea

base level provided by the Kansas River. Throug

the basin several other causes contributed, or pote

tially contributed, to channel changes along Soldi

Creek including additional channel modifications 

example, low-water crossings, weirs, bridge work

land-use change, floods, and climate change.
22 Historical Channel Change Along Soldier Creek, Northeast Kansas

Upstream from Rocky Ford, the most recently available information indicated that the channel bed had

become relatively stable at all gaging-station sites. As

of 2001, the available evidence indicated that Soldier

Creek at and upstream from Rocky Ford has not been

substantially affected by the upstream-progressing

channel-bed degradation.

The channelization of Soldier Creek, completed in

1961, caused substantial channel change at the Soldier

Creek gaging station near Topeka, which is located

within the channelized section. Immediate channel

changes at this station included a decrease in channelbed elevation of about 5 ft and an increase in channel

width of about 35 ft. Subsequently, from 1962 to 1999,

the channel bed continued to degrade at an average

rate of about 0.03 ft/yr.

The instability introduced by the channelization

of Soldier Creek caused channel-bed degradation

that progressed upstream at the rate of about 0.7 to

1.2 mi/yr. At the Soldier Creek gaging station near

Delia, which is located about 12 stream mi upstream

from the upstream end of the channelized section,

channel-bed degradation began following the partial

washout of a downstream low-water crossing in 1978.

As of 1999, the channel bed at the gaging station near

Delia had degraded 5.1 or 6.6 ft (depending on

whether the sediment deposited upstream from the

low-water crossing is included or discounted in the

calculated change) at an average rate of about 0.2 or

0.3 ft/yr, and channel-bed degradation as of 1999 had

not yet begun to slow.

At Rocky Ford, a bedrock outcrop in the Soldier

Creek channel that is located about 6.8 stream mi

upstream from the Delia gaging station and within the

Prairie Band Potawatomi Nation Reservation, the

upstream progression of channel-bed degradation

potentially began to affect the channel in the mid1980s. However, a lack of increase in the height of the

low-flow waterfall at Rocky Ford indicated that the

channel bed immediately downstream has yet to be

degraded substantially as of 2001. A combination of

natural and human-caused conditions may have limited the upstream progression of channel-bed degradation. However, it is not known if the limitation is

complete or partial, permanent or temporary. It is

possible that with more time channel-bed degradation

immediately downstream from Rocky Ford may

become more evident. The bedrock outcrop in the

channel at Rocky Ford should minimize the r

channel-bed degradation upstream from the s

This assessment determined that the chan

degradation caused primarily by the channeli

Soldier Creek had migrated upstream at least 

the Delia gaging station and potentially may b

ing the channel within the reservation immed

downstream from Rocky Ford. Long-term mo

of channel conditions at and immediately dow

from Rocky Ford may provide the informatio

sary to determine the magnitude and rate of c

bed degradation should it occur in the future. 

monitoring, at a minimum, should include the 

remeasurement of the height of the waterfall 

Ford during low-flow conditions. Ideally, the 

ing also would include the establishment and 

resurvey of several monumented cross section

more comprehensively assess channel change

Because degradation of Soldier Creek ma

causes other than the channelization, especial

upstream from Rocky Ford, additional investi

may be warranted. For example, a low-altitud

reconnaissance and acquisition of photograph

low-flow, leaf-off conditions, coupled with th

historical aerial photographs, may provide som

information needed to comprehensively deter

locations of channel degradation along Soldie

The aerial photographs potentially could be u

determine the timing and location of bank col

which then could be investigated in relation to 

potential causes including human disturbance

streamflow, the composition of the channel be

banks, channel geometry, and vegetation. A c

hensive analysis of streamflow characteristic

ing the frequency and “flashiness” of high flo

may provide important information for under

the hydrology and stability of the Soldier Cre

system. Related studies (perhaps involving a m

approach), which may provide important info

for understanding storm runoff within the bas

include analyses of sediment loads, basin cha

tics (for example, soils, land use, slope), and 

management practices (for example, terraced 

unterraced cropland). Together, such studies w

provide information necessary for improved u

standing and management of the Soldier Cree

system.
References 

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