Dendrogeomorphic Estimate of Changes in 

Sedimentation Rate Along the Kankakee River 

Near Momence, Illinois

Sy Richard L Phipps, Gary P. Johnson, and Paul J. Terrio

U.S. GEOLOGICAL SURVEY

Water-Resources Investigations Report 94-4190

Prepared in cooperation with the

KANKAKEE SOIL AND WATER CONSERVATION DISTRICT

Urbana, Illinois 

1995
U.S. DEPARTMENT OF THE INTERIOR 

BRUCE BABBITT, Secretary

U.S. GEOLOGICAL SURVEY 

Gordon P. Eaton, Director

For additional information Copies of this report can be

write to: purchased from:

District Chief U.S. Geological Survey-ESIC

U.S. Geological Survey Open-File Reports Section

102 E. Main St., 4th Floor Box 25286, MS 517

Urbana, IL 61801 Denver Federal Center

	Denver, CO 80225-0046
CONTENTS

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

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

Purpose and Scope.............................................................................. 3

Description of the Study Area ..................................................................... 3

Acknowledgments .............................................................................. 5

Dendrogeomorphic Estimate of Changes in Sedimentation Rates .............................................. 5

Site Selection.................................................................................. 8

Data Collection ................................................................................ 9

Data Presentation and Analysis .................................................................... 9

Interpretation of the Data......................................................................... 21

Summary and Conclusions............................................................................. 28

References Cited .................................................................................... 28

Glossary........................................................................................... 30

FIGURES

1-2. Maps showing:

1. The Kankakee River Basin in Illinois and Indiana, the Momence Wetland, and streamflow- and raingaging stations. .......................................................................... 2

2. The locations of the six data-collection sites within the study area in the Momence Wetland, Illinois

and Indiana ............................................................................. 4

3. Diagram showing a tree in a flood plain and increment borer. .......................................... 6

4. Photograph showing trees resembling utility poles in a flood plain ...................................... 7

5. Graph showing relation of sediment depth to tree age, Site 1 near Momence, 111. ........................... 11

6. Distributions of tree ages at the six data-collection sites and net sedimentation rates for trees in various age

groups in the Momence Wetland near Momence, 111. ................................................. 13

7-11. Graphs showing:

7. Relation of sediment depth to tree age, Site 2 near Momence, 111.................................... 14

8. Relation of sediment depth to tree age, Site 3 near Momence, 111.................................... 16

9. Relation of sediment depth to tree age, Site 4 near Momence, 111.................................... 18

10. Relation of sediment depth to tree age, Site 5 near Momence, 111.................................... 20

11. Relation of sediment depth to tree age, Site 6 near Momence, 111.................................... 22

12. Plots showing mean annual discharge at four streamflow-gaging stations in the Kankakee River Basin

through 1992 ................................................................................ 24

13. Total annual precipitation, Wheatfield, Ind., 1921-91................................................. 25

14. Total annual precipitation, Plymouth, Ind., 1922-92.................................................. 26

TABLES

1. Dendrogeomorphic data collected at Site 1 near Momence, 111. ......................................... 10

2. Pre-1950 and post-1950 sedimentation rates at Site 1 near Momence, 111................................... 12

3. Dendrogeomorphic data collected at Site 2 near Momence, 111. ......................................... 15

4. Pre-1950 and post-1950 sedimentation rates at Site 2 near Momence, 111.................................. 15

5. Dendrogeomorphic data collected at Site 3 near Momence, 111. ......................................... 15

6. Pre-1950 and post-1950 sedimentation rates at Site 3 near Momence, 111.................................. 17

7. Dendrogeomorphic data collected at Site 4 near Momence, 111. ......................................... 17

8. Pre-1950 and post-1950 sedimentation rates at Site 4 near Momence, 111.................................. 17

9. Dendrogeomorphic data collected at Site 5 near Momence, 111. ......................................... 19

10. Pre-1950 and post-1950 sedimentation rates at Site 5 near Momence, 111.................................. 19

11. Dendrogeomorphic data collected at Site 6 near Momence, 111. ......................................... 21

Contents III
CONTENTS

12. Pre-1925, 1925-50, and post-1950 sedimentation rates at Site 6 near Momence, 111.......................... 21

13. Summary of net sedimentation rates at data-collection sites near Momence, 111............................. 23

14. Estimated period of inundation of data-collection sites along the Kankakee River near Momence, 111. .......... 27

CONVERSION FACTORS

Multiply By To obtain

millimeter (mm) 0.03937 inch

centimeter (cm) .3937 inch

meter (m) 3.281 foot

kilometer (km) .6214 mile

square kilometer (km2) .3861 square mile

cubic meter per second (m /&) 35.31 cubic foot per second

centimeter per kilometer (cm/km) .6336 inch per mile

centimeter per year (cm/yr) .3937 inch per year

hectare (ha) 2 471 acre

IV Contents
Dendrogeomorphic Estimate Of Changes In 

Sedimentation Rate Along The Kankakee River 

Near Momence, Illinois

by Richard L. Phipps, Gary P. Johnson, and Paul J. Terrio

Abstract

Changes in sedimentation rates were estimated using root-burial depth and tree-age data 

at six selected data-collection sites along the 

Kankakee River near Momence in Kankakee 

County, Illinois. Five sites were in backwater 

areas away from the river channel, and one site 

was on a natural levee near the channel.

A summary of the dendrogeomorphic data 

at the six sites indicates that sedimentation rates 

were greater after 1950 than before 1950. 

Greater sedimentation rates after 1950 were 

observed at four of the five backwater sites, 

whereas no change in sedimentation rate after 

1950 was observed at the fifth backwater site. 

The observed rates could have been affected by 

any combination of soil erosion, soil compaction, 

or increased streamflow. A greater sedimentation rate after 1950 was observed at the levee site, 

which appeared to have been affected by erosion 

from a flood in 1950. Effects of erosion were 

not observed at any of the other sites. No erosional effects and soils not susceptible to compaction at the five backwater sites indicate that 

neither erosion nor compaction affected observed 

sedimentation rates. The effect of increased 

streamflow in the Kankakee River Basin since 

the early 1900's on the observed sedimentation 

rates is not known.

INTRODUCTION

The Kankakee River originates near South 

Bend, Ind., and joins the Des Plaines River southwest 

of Chicago near Wilmington, 111., to form the Illinois 

River (fig. 1). Historical evidence indicates that 

De La Salle and Father Hennipen, who traveled down 

the river in 1679, were probably the first Europeans to 

see the Kankakee River (Houde and Klasey, 1968). 

At that time, the meandering upper part of the river 

was a 5- to 8-km-wide marsh presently referred to 

as a riverine wetland. The river and bordering 

wetlands extended from the headwaters in Indiana 

to Momence, 111. The river downstream from 

Momence, then as now, had fewer meanders and 

was not bordered by wetlands. As the region 

was settled, the riverine wetland, unsuitable for 

agriculture, was at first left undrained and was 

referred to as the Grand Marsh, a prime area for 

hunting and fishing.

From the time of settlement, the Kankakee 

River Basin outside the Grand Marsh has been intensively farmed. Houde and Klasey (1968) note that 

by "around 1860" parts of the river in Indiana were 

being channelized for draining the marsh and reducing 

the extent and frequency of flooding. By 1918, the 

entire main stem of the river in Indiana had been 

completely channelized (U.S. House of Representatives, 1916 and 1931). The channelization reduced 

the length of the river in Indiana from about 385 km 

to about 130 km. The reduction in length greatly 

increased the gradient of the Indiana part of the river. 

The average gradient of the prechannelized Kankakee 

River was estimated to be about 8 cm/km. After 

channelization, the average gradient was estimated to

Introduction
0.

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EXP

MOMENCE 

BASIN BO

STREAMF

RAIN-GAG

CITY

Kankakee

River

Basin

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Figure 1. The Kankakee River Basin in Illinois and Indiana, the Momence Wetland, and streamflow- and rain-gaging stati
be 16 cm/km (U.S. House of Representatives, 1916 

and 1931). This converted the meandering river 

through the Grand Marsh to channels that drained 

the marsh and permitted conversion of much of its 

original acreage to agricultural use. The main 

stem of the river was not channelized between the 

State line and Momence, and this area continued to 

experience frequent flooding and a high water table. 

These conditions made agriculture in the area 

impractical. The area has remained a forested 

wetland and is known locally as the Momence 

Wetland (fig. 1).

Sedimentation of the Illinois part of the Kankakee River has been a major local concern for many 

years. Local residents are concerned that sedimentation limits recreational, ecological, and the aesthetic 

usefulness of the river and contend that sand is being 

moved and deposited at faster than natural rates in the 

channel. The Illinois State Water Survey (ISWS) and 

the Illinois State Geological Survey (ISGS) investigated the Illinois part of the river in the late 1970's and 

early 1980's (Bhowmik and others, 1980; Bhowmik 

and Bogner, 1981; Gross and Berg, 1981). They 

agreed that extensive drainage of the Grand Marsh 

wetlands and channelization of the main stem of the 

Kankakee River had caused increased sedimentation 

downstream from the State line. Utilizing information gathered from aerial photographs and topographic 

maps, Gross and Berg (1981) concluded that by the 

early 1950's the river had reached equilibrium; consequently, further increases in sedimentation rates in 

the Illinois part of the river should not be expected. 

Bhowmik and others (1980) expressed concern that 

conclusions regarding sedimentation stabilization had 

been based on no more than 2 years of data. Ivens 

and others (1981) commented that, because of such 

relatively short records, the equilibrium interpreted 

from the data may only represent a temporary condition. Local residents have continued to express 

concern that sedimentation has not reached equilibrium but has continued to increase during the last few 

decades. In 1992, the U.S. Geological Survey 

(USGS), in cooperation with the Kankakee Soil and 

Water Conservation District, began a study to investigate changes of sedimentation rates over time on the 

flood plain of the Kankakee River near Momence, 

Kankakee County, 111.

Purpose and Scope

This report presents results of a study utilizing 

dendrogeomorphic techniques to estimate changes 

in sedimentation rates along the Kankakee River. 

Recent sedimentation rates are placed into perspective 

by describing the trend in historical sedimentation 

rates. Tree ages in conjunction with burial depths 

of tree roots were utilized to estimate past sedimentdeposition rates at selected sites on the flood plain 

of the Kankakee River near the Illinois-Indiana State 

line. Data were collected during the summer of 

1992. Some description of the hydrologic conditions 

for the period of record at four streamflow-gaging 

stations in the Kankakee River Basin also is included.

Description of the Study Area

The Momence Wetland between the State line 

and Momence, 111., is largely an undisturbed forested 

area. The area is frequently inundated by the Kankakee River and, therefore, subject to sediment deposition. For this reason, the area was chosen as the 

initial site for the dendrogeomorphic study.

The study area includes six sites in the floodplain forest of the Momence Wetland within 2 km 

of the Illinois-Indiana State line near Momence, 111. 

(fig. 2), and is a wet area variant of the typical elmash-maple flood-plain forest found along streams 

throughout the Midwest. The Momence Wetland 

is dominated by silver maple (Acer saccharinum L. 1 ). 

Other species coexist with the maple in specific 

habitats, but silver maple seems to be the most abundant tree species in the wetland. The understory is 

often quite open with sparse herbaceous vegetation 

except in very moist or disturbed areas. The ground 

surface in moist areas may be bare or covered by a 

dense stand of lizard's-tail (Saururus cernuus L.). 

Much of the understory contains an abundance of wild 

grape (Vitis spp.).

Many old cutoff meanders are distinguishing 

features of the landscape. The former meanders 

contain standing water, the surface elevation of which 

appears to be controlled by the elevation of the water 

in the nearby river channel. Rose mallow (Hibiscus

'Nomenclature of trees follows that of Little (1979); all other 

plant nomenclature follows that of Gleason (1952).

Introduction
87° 32' 30" 87° 32' 87° 31' 30"

!

o

o

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41° 10'

41° 09' 30" 

EXPLANATION

 I DATA-COLLECTION SITES 

EZJ OPEN WATER

0.5 MILE

0.5 KILOMETER

Figure 2. The locations of the six data-collection sites within the study area in the Momence Wetland, Illinois and Indiana.
palustris L.) and a band of buttonball bush (Cephalanthus occidentalis L.) often ring the open, standing 

water of these old backwater meanders. The major 

tree species nearest the meanders (sometimes intermixed with the buttonball bush) is silver maple, 

although there might also be green ash (Fraxinus 

pennsylvanica Marsh.). Ash trees increase in 

abundance farther from the standing water. The 

maple forest around the backwater meanders could 

be described as an ash-maple phase of the elm-ashmaple flood-plain forests.

Oaks are found with silver maples in areas 

at slightly higher elevations that are less frequently 

flooded than the areas adjacent to meanders. The 

oaks almost always include swamp white oak 

(Quercus bicolor Willd.), with bur oak (Q. macrocarpa Michx.) and pin oak (Q. palustris Muenchh.) 

likely present but less abundant. Better drained 

sandy areas, such as natural levees along the channel, 

have elm (Ulmus americana L.) as the predominant 

species intermixed with the ubiquitous silver maple. 

The forest of the natural levees could be described as 

an elm-maple phase of the elm-ash-maple flood-plain 

forests.

Acknowledgments

Much assistance with this project was provided 

by a local confederation of citizen groups known as 

The Alliance to Restore the Kankakee (ARK). The 

endless enthusiasm of ARK for this project, and the 

eagerness of its membership to help in any way possible, is gratefully acknowledged.

DENDROGEOMORPHIC ESTIMATE OF 

CHANGES IN SEDIMENTATION RATES

Sigafoos (1964) demonstrated that sedimentation rates on flood plains could be determined by 

excavating root systems and by taking increment 

cores for age determination from trees in flood plains. 

The burial depth of the original lateral roots of a tree is 

an estimate of the amount of sediment deposited, and 

the age of the tree estimates the length of time during 

which the sediments accumulated (fig. 3). By examining a number of trees of various ages, the relation 

between net sedimentation depth and time can be 

examined. This dendrogeomorphic technique has

since been applied in western Tennessee (Hupp and 

Bazemore, 1993), along the Cache River in eastern 

Arkansas (Hupp and Morris, 1990), and in riverine 

wetlands in southeastern Virginia (Hupp and others, 

1993). The methods utilized in this study follow 

those described in Hupp and Bazemore (1993).

Tree seedlings normally develop lateral roots 

just below, and parallel to, the soil surface. When 

sediments are deposited around trees in wetlands, the 

water level in the soil is not necessarily raised appreciably. Thus, the original roots are not killed by 

water saturation from a raised water level in the soil. 

Further, no lateral roots are typically found below the 

original lateral roots because there is no tap root from 

which they could grow. The original lateral roots or 

their locations can be identified in many wetland tree 

species, even though the root systems of the trees may 

be buried by a meter or more of accreted sediment. 

Because the original lateral roots were formed just 

below the surface on which the seedling became established, the depth of sediment from the present surface 

to the level of the original lateral roots is an approximation of the net depth of sedimentation since the 

establishment of the seedling. By determining the 

age of the tree, the net sedimentation rate for a given 

time interval (the age of the tree) can be determined.

Trees in areas where appreciable amounts of 

sediment are deposited become partially buried by the 

sediment. Burial may completely cover the root 

crown at the base of the tree. The trunks of such 

trees are similar to utility poles, with no root crown 

exposed above the soil surface (fig. 4). Many trees in 

and around the backwater meanders of the study area 

have this appearance.

Sedimentation after the establishment of the 

seedling usually results in new roots being formed in 

the sediment deposits above the original lateral roots. 

These new roots form as root sprouts (adventitious 

lateral roots) (fig. 3) from the buried part of the tree 

trunk (main stem). The new roots tend to be horizontal, as were the original lateral roots, and may be 

mistaken for the original roots.

The development of any particular root depends 

on a variety of factors and conditions, such as rate and 

frequency of sediment-deposition events, soil drainage, and depth to water table during the growing 

season. Roots at all levels are sometimes found to be 

about the same size. Alternatively, roots at a particular level will sometimes grow larger than roots at other 

levels. The largest lateral roots might be at the level

Dendrogeomorphic Estimate of Changes in Sedimentation Rates 5
INCREMENT 

BORER

PRESENT GROUND SURFACE

ADVENTITIOUS ROOTS

ACCRETED SEDIMENT

^SGROUND SURFACE 

AT TIME OF SEEDLING

ORIGINAL LATERAL ROOTS

Figure 3. A tree in a flood plain and increment borer.

6 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
Figure 4. Trees resembling utility poles in a flood plain.

of the original lateral roots or might be any roots above 

the original roots. Sometimes lateral roots at the 

level of the original roots may be small and difficult 

or impossible to detect. In such cases, the point 

below which no more vertical stem can be detected 

is assumed to be the level of the original roots, and, 

hence, an approximation of the level of the surface 

on which the seedling became established.

The sedimentation rate is estimated from the 

amount of sediment measured at a particular time, 

without regard to when the sediment was deposited. 

The resulting estimates of sedimentation rate, therefore, represent net sedimentation rates over the lifetime of the tree, without consideration of when the 

sediments were deposited. The sediments could 

have been in place for decades or could have been 

deposited during the most recent flood prior to 

sampling.

By determining whether the historical trend 

of sediment deposition on the flood plain has been 

increasing, decreasing, or remaining stable, the

trend of sand movement in the channel can be inferred. 

During floods, water overflows the channel and sediments might be deposited on the flood plain. Sand 

(sediment particles between 0.062 and 2.0 mm in 

diameter) is heavy enough that it is typically transported along or near the bottom, or bed, of river 

channels. In the Kankakee River, sand transport 

is largest during floods (Bhowmik and others, 1980), 

although some sand is moved slowly along the channel 

bed during most flow conditions. Therefore, the 

historical trend of sand movement in the channel 

might be reflected in the depositional trend of sediments on the flood plain.

The dendrogeomorphic analyses for this study 

were done with samples from depositional areas and 

do not provide a quantitative analysis of the entire 

flood plain. No attempt was made to determine what 

part of the flood plain or channel was depositional and 

what part was erosional. Thus, determination of 

change in sedimentation rate over time should not be 

related to the amount of sediment deposited on the

Dendrogeomorphic Estimate of Changes in Sedimentation Rates
flood plain or the amount of sediment transported in 

the river channel. Only under certain conditions 

could the analyses be applied to quantify sediment 

transport in the channel or sedimentation rate for the 

entire flood plain. The dendrogeomorphic analyses 

for this study examine whether the rate of sediment 

deposition has increased, decreased, or remained 

constant over time in areas of known deposition.

Site Selection

Four factors were used in selecting sites along 

the Kankakee River to collect sediment depth and tree 

age data. First, an appreciable thickness of sediment 

deposited during the lifetime of the trees growing on 

the site was needed for analysis. Although using 

sites where there was no sediment accretion would 

have helped to determine areas of deposition and 

erosion, such sites would not provide data on changes 

in sedimentation rates. Because a large part of the 

sediment in the Kankakee River is sand, sand deposits 

were sought. The few forested sand deposits found 

were within 4 km downstream from the IllinoisIndiana State line and within about 20 m of the 

channel.

Forested sites with relatively large amounts of 

sediment deposits were difficult to find. Localized 

areas of sediment deposition were not typical of the 

entire flood plain. According to Bhowmik and others 

(1980, p. 81):

"It appears that during flood stages, when the 

velocity of water is relatively high and the water is 

very turbulent, most of the suspended sediment 

carried by the river consists of sandy materials."

This statement was made in reference to movement of 

sediment in the channel. Much of the water that 

leaves the channel and spreads across the broad flood 

plain moves relatively slowly. The slow-moving 

water across the flood plain cannot transport sandy 

material, and only finer sediment (silt and clay) is 

deposited on the flood plain. Few forested areas 

of deposition and few forested areas with erosional 

features were found during this study.

Areas surrounding old cutoff meanders in the 

backwater areas away from the river channel contained the most prominent depositional features. 

The old cutoff meanders, locally called sloughs,

were scattered along both sides of the river between 

the State line and Momence (fig. 2). Most of the 

backwater cutoff meanders are in undisturbed, undeveloped, forested areas. Sediments are deposited 

among the trees near the meanders and deposits 

increase in thickness toward the standing water in 

the center of each backwater area, indicating that 

the sediments slowly settled from ponded flood water. 

Five of the six data-collection sites were in these backwater areas.

Second, an acceptable site had to contain trees 

of species from which reliable data could be obtained. 

The most reliable data were collected from ash trees 

near the Kankakee River. Though oaks also were 

acceptable, few were found at most acceptable sites 

along the river. At some potential sites, ash trees 

were present but too widely scattered to utilize. 

Silver maples were present at most depositional areas. 

Unfortunately, unlike the ash, the original lateral roots 

of the silver maple were very hard to distinguish. 

The ease of finding the seedling root location of ash 

trees was dependent on the development of the root 

system. If the soil was well drained, then roots that 

began at the level of the original lateral roots may have 

grown outward and downward to depths below the 

original lateral roots. Wright (1959) refers to the 

extensive root system of green ash that, under favorable conditions, may penetrate to 1.4 m but makes no 

reference to a tap root. No ash-tree roots were 

observed resembling a tap root. No evidence that 

any of the roots were attached below the original 

lateral roots was found; thus, the positions of the 

original lateral roots were distinct.

Third, several trees representing a range of 

ages had to be contained in an acceptable site in order 

to estimate changes in sedimentation rates. The 

depth of sediment that accumulated during the lifetime 

of an old tree does not in itself indicate whether the 

sedimentation rate has increased or decreased during 

the lifetime of the tree; it only indicates the net total 

deposition during the lifetime of the tree. The measured net deposition could have been affected by any 

combination of depositional or erosional processes. 

If sedimentation rates have increased with time, then 

net sedimentation rates from older trees will be biased 

to greater values because of recent greater sedimentation rates. Likewise, if present sedimentation rates 

are smaller than in the past, the net sedimentation rates 

for older trees will be biased to lesser values. To

8 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
determine whether or not deposition may have increased during the last few decades, emphasis was 

placed on finding sites with trees of various ages.

Fourth, several trees of an acceptable species 

that were fairly close together to minimize natural 

variability of sedimentation rates had to be contained 

across an acceptable site. The amount of sediment 

deposited per unit time (sediment depth divided by 

tree age, D/A) varied considerably from one site to 

another. For this reason, the size of the sites was kept 

relatively small (about 0.4 ha) so there was little 

chance of significant depositional variation across the 

site.

The combined effect of these four factors 

effectively reduced the number of potential sites. 

Resulting acceptable sites were generally depositional 

areas around backwater ponds that contained a group 

of ash trees of variable ages.

Data Collection

Sediment depth was determined as the distance 

from the present soil surface to the level of the original 

lateral roots. Holes were dug on opposite sides of 

each tree from which data were to be collected. If 

sediment depths on opposite sides were markedly 

different, or otherwise seemed questionable, one of 

the holes was enlarged or a third hole was dug to allow 

for a more careful examination of root distribution. 

Numerous smaller elms were completely excavated 

and taken to the laboratory for examination and measurement. If the roots were large, then the depth 

measurement was made to the approximate center 

of the roots. Measurements were taken about 0.5 m, 

laterally, from the center of the tree, though this distance varied depending on the size of the tree. Sediment depths were measured to the nearest centimeter. 

Although the measurement of the level of the original 

lateral roots and the level of the soil surface directly 

above the point of the root measurement could be 

inexact, repeated measurements by USGS personnel 

almost always were within 1 cm of the original measurement. After the data were collected, the holes 

were filled and the trees were tagged for possible 

future reference.

Tree age was estimated by counting rings from 

an increment core of the tree, and then estimating the 

number of rings at the center that were not included 

on the core sample. Typically, a single core was

extracted with an increment borer (fig. 3) from each 

sample tree and the age of the tree was determined by 

examining the core under a dissecting microscope in 

the laboratory. Increment cores were usually taken 

from standard breast height (1.4 m) for larger trees and 

from as near to the present soil surface as practicable 

for smaller trees. Rings near the centers of the trees 

were usually large, indicating rapid growth in trunk 

diameter in youth. Rapid growth in diameter implies 

rapid growth in height, and rapid growth in height 

indicates that the difference in age determinations 

between samples taken at ground level and those taken 

at breast height would be small. Age determinations 

were done on some trees from both breast height and 

near the ground surface, and little or no difference was 

found in the age determinations. Sample height, side 

of the tree sampled, and tree diameter were recorded 

for each tree. Increment cores were taken and 

processed in accordance with standard procedures 

(Phipps, 1985).

Data Presentation and Analysis

Site 1, where the youngest trees were found, 

was located on a natural sand levee at an inside bend 

on the north side of the Kankakee River (fig. 2). This 

site was well drained and may be described as an 

elm-maple site. Most of the trees sampled at this site 

were elm. Because the original rooting level of elms 

are less easily determined than those of ash, emphasis 

was placed on sampling any ash that were present.

The data from Site 1 are presented in table 1. 

Numerous trees were relatively small and were 

completely excavated. In the well drained soil of 

the levee, some of the elms developed what appeared 

to be a short tap root. This is consistent with a study 

by Guilkey (1957) that noted the American elm can 

develop a tap root in deep, well drained soils. When 

these roots were present, it was usually not possible to 

determine the position of the original lateral roots. 

Data from these trees are not included in table 1, 

resulting in gaps in the numbering system.

The ages of the trees at Site 1 ranged from 9 to 

69 years. The thickness of sediment covering the 

original lateral roots of older trees generally increased 

with tree age, but distinct exceptions were noted, as 

illustrated by the relation of sediment depth to tree age 

for the first three trees listed in table 1. Of these trees 

(BS2-1, BS2-2, and BS2-5), tree BS2-1 was 13 years

Dendrogeomorphic Estimate of Changes in Sedimentation Rates 9
Table 1. Dendrogeomorphic data collected at Site 1 near Momence, III.

[cm, centimeters; cm/yr, centimeters per year; --, no data available]

Dbh: Diameter at breast height (1.4 meters).

Inside date: Date of innermost tree ring. Number in parentheses is estimated number of missed

center rings; p indicates that the pith was reached in the core. 

Tree age: Age including minimum number of missed center rings. 

Sediment depth: Net sediment accumulation during lifetime of tree. 

D/A: Sediment depth divided by tree age (net sedimentation rate). 

Tree species: Either ash (Fraxinus) or elm (Ulmus).

Tree 

number

BS2-1

-2

-5

-6

-9

-10

-11

-12

-13

-14

-16

-18

-21

-22

-23

-24

-25

. -26

-27

-29

-31

-32

-34

Dbh

_

12

7

7

8

13

8

 __^

-

-

-

9

--

-

25

25

41

14

~

--

 --

- '

Inside date

1980 (p)

1958 (4)

1958 (1-2)

1958 (p)

1972(1)

1939 (p)

1957 (p)

1956 (p)

1980 (p)

1934(1-2)

1981 (p)

1934(1-2)

1953 (p)

1924 (p)

1957 (p)

1954 (p)

1958 (2-3)

1971 (2-3)

1955 (p)

1984 (p)

1960(1)

1957 (p)

1963 (p)

Tree 

age 

(years)

13

39

36

35

22

54

36

37

13

60

12

60

40

69

36

39

37

24

38

9

34

36

30

Sediment 

depth 

(cm)

15

13

38

44

30

16

10

18

20

18

11

27

37

22

27

32

32

27

29

27

48

36

34

D/A 

(cm/yr)

1.2

.33

1.1

1.3

1.4

.30

.28

.49

1.5

.30

.92

.45

.93

.32

.75

.82

.86

1.1

.76

3.0

1.4

1.0

1.1

Tree 

species

Elm

Elm

Ash

Elm

Elm

Elm

Elm

Elm

Elm

Ash

Elm

Elm

Ash

Elm

Ash

Ash

Ash

Elm

Elm

Elm

Elm

Elm

Elm

old and 15 cm of sediment covered the roots, and 

tree BS2-5 was 36 years old and 38 cm of sediment 

covered the roots. It appears that sediment was accumulating at these trees at a rate of about 1 cm/yr. On 

the other hand, tree BS2-2 was the oldest of the three 

trees (39 years) but the amount of sediment deposited 

(13 cm) was the least for the three trees; a few disparities between tree age and sediment depth may be 

normal and natural; however, this disparity is extreme 

and is discussed below.

The relation of depth of sediment to tree age 

at Site 1 underwent a distinct shift about 35 to 40 years 

ago as shown in figure 5. Because of the limited 

number of data, a linear best-of-fit line was determined to describe the relation of depth of sediment to 

tree age for periods before and after the distinct shift in 

this relation. A flood in 1950 seems to have removed

20 cm or more of sediment from Site 1. Streamflow 

records indicate a maximum discharge for the period 

of record on April 25, 1950, at the streamflow-gaging 

station at the Kankakee River at Momence (U.S. Geological Survey, 1964, p. 450), which could have 

removed sediment from Site 1. From these data 

alone, it is not known if sediment was eroded at Site 1 

every time the levee was overtopped, or if sediment 

was eroded only during extreme floods. If the latter 

is the case, little sediment may have been eroded 

during the lifetimes of the younger trees.

Data for the first three trees shown in table 1 

(BS2-1, BS2-2, and BS2-5) are identified in figure 5. 

Trees BS2-1 and BS2-5 appear to have developed on 

the ground surface after the erosional event, and tree 

BS2-2 appears to have become established on the 

newly eroded, unstable surface. The condition of this

10 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
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Data Presentation and Analysis 11
surface would account for both the relatively large 

number of trees established 30 to 40 years ago and the 

apparent variation in amount of sediment deposition 

among trees established during those years.

The data from Site 1 (table 1) were separated 

into two age groups to represent trees that became 

established either before or after 1950. Computed 

values of the net sedimentation rate at each tree are 

included in table 1, whereas the average sedimentation 

rates for the two age groups are included in table 2. 

The net sedimentation rates of the pre-1950 trees were 

likely biased to smaller values by the apparent erosion 

in 1950. ;

If it is assumed that erosion around trees established before 1950 was due largely to the 1950 flood, 

and that the amount of sediment eroded around all 

trees at Site 1 was essentially the same, adding a 

constant depth to all of the older trees to compensate 

for the 1950 erosional event would allow for better 

comparison of the two groups. Regression lines 

defining the slope of sediment deposition and tree 

age for periods before and after 1950 (fig. 5) indicate 

that the net sedimentation rate since 1950 was greater 

(steeper slope of regression line) than prior to 1950.

Reasons other than the apparent erosion at Site 1 

during the flood of 1950 also justified separating the 

data into two groups. Studies completed around 

1980 reported that the Kankakee River was near equilibrium around 1950, and that no further increases in 

sedimentation should be seen (Gross and Berg, 1981; 

Ivens arid others, 1981). In addition, the data from 

every site, when separated into groups of trees established before and after 1950, also show a division 

around 1950 (fig. 6). For these reasons, 1950 was 

used to divide data from each site for comparison of 

sedimentation rates.

Site 2 was on the north side of the channel, 

downstream from Site 1 (fig. 2) in an area where no 

erosional features were present. Site 2 was near a 

backwater cutoff meander and may be described as an

ash-maple site. The data for Site 2 are presented in 

table 3 and are shown graphically in figure 7. Tree 

ages ranged from 28 to 47 years, with net sediment 

deposition during the lifetimes of the trees that ranged 

from 14 to 25 cm. The data were divided into two 

groups of trees established before or after the 1950 

flood (table 4). A smaller difference in net sedimentation rate from Site 1 between the pre- and post-1950 

groups resulted at Site 2. The pre-1950 group still 

had a smaller net sedimentation rate (0.42 cm/yr) than 

the post-1950 group (0.54 cm/yr). The smaller net 

sedimentation rate of the pre-1950 period could have 

been caused by recent erosion, but no active erosional 

features were present.

Site 3 also was on the north side of the channel, 

but farther from the channel than Site 1 (fig. 2). This 

was an ash-maple site near a backwater cutoff meander quite similar to Site 2. The trees sampled ranged 

in age from 34 to 60 years, and the net sediment deposition during the lifetimes of the trees ranged from 22 

to 30 cm (table 5). As with Site 2, the range of tree 

age and sediment depth are relatively narrow. The 

data are graphically shown in figure 8 and are summarized into the pre- and post-1950 age groups in table 6. 

Again, the age and sediment data indicate that sediments may have been accumulating at a larger rate in 

more recent years. The smaller net sedimentation 

rate of the pre-1950 period indicates that there might 

have been some erosion during the period, but no 

active erosional features were found.

Site 4 was in an ash-maple site on the south side 

of the channel, adjacent to a small ditch between a 

backwater cutoff meander and the channel (fig. 2). 

All trees sampled at this site were ash. Tree ages 

ranged from 32 to 76 years, and sediment accumulation during the lifetimes of the trees ranged from 13 

to 64 cm (table 7). All data are shown in figure 9. 

The data were then summarized into pre- and 

post-1950 age groups (table 8). Erosion was not 

evident at Site 4, as was noted for Site 1 on the north

Table 2. Pre-1950 and post-1950 sedimentation rates at Site 1 

near Momence, III.

[D/A, sediment depth divided by tree age; cm/yr, centimeters per year]

Group

Pre-1950

Post- 1950

Number 

of 

trees

4

19

Age 

range 

(years)

54-69

9-40

Year range 

(years of 

germination)

1924-39

1953-84

D/A range 

(cm/yr)

0.30-0.45

0.28-3.0

Average 

D/A 

(cm/yr)

0.34

.93

12 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
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N14 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
Table 3. Dendrogeomorphic data collected at Site 2 near Momence, III.

[cm, centimeters; cm/yr, centimeters per year] 

Dbh: Diameter at breast height (1.4 meters). 

Inside date: Date of innermost tree ring. Number in parentheses is estimated number of

missed center rings; p indicates that the pith was reached in the core. 

Tree age: Age including minimum number of missed center rings. 

Sediment depth: Net sediment accumulation during lifetime of tree. 

D/A: Sediment depth divided by tree age (net sedimentation rate). 

Tree species: Either ash (Fraxinus) or elm (Ulmus).

Tree 

number

BS3-1

-2

-3

-4

-5

-6

-7

Dbh

38

22

18

21

13

23

23

Inside date

1946 (p)

1949 (0-1)

1946 (p)

1955 (0-1)

1965(0-1)

1953(0-1)

1962 (p)

Tree 

age 

(years)

47

44

47

38

28

40

31

Sediment 

depth 

(cm)

18

21

19

25

17

IS

14

D/A 

(cm/yr)

0.38

.48

.40

.66

.61

.45

.45

Tree 

species

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Table 4. P re-1950 and post-1950 sedimentation rates at Site 2

near Momence, III.

[D/A, sediment depth divided by tree age; cm/yr, centimeters per year]

Group

Pre-1950

Post- 1950

Number 

of 

trees

3

4

Age 

range 

(years)

44-47

28-40

Year range 

(years of 

germination)

1946-49

1953-65

D/A range 

(cm/yr)

0.38-0.42

0.45-0.66

Average 

D/A 

(cm/yr)

0.42

.54

Table 5. Dendrogeomorphic data collected at Site 3 near Momence, III.

[cm, centimeters; cm/yr, centimeters per year] 

Dbh: Diameter at breast height (1.4 meters). 

Inside date: Date of innermost tree ring. Number in parentheses is estimated number of

missed center rings; p indicates that the pith was reached in the core. 

Tree age: Age including minimum number of missed center rings. 

Sediment depth: Net sediment accumulation during lifetime of tree. 

D/A: Sediment depth divided by tree age (net sedimentation rate). 

Tree species: Either ash (Fraxinus) or elm (Ulmus).

Tree 

number

BS4- 1

-2

-3

-4

-5

-6

Dbh

23

33

22

27

22

12

Inside 

date

1934(0-1)

1934(1-2)

1935(0-1)

1953 (p)

1946(2-3)

1959 (p)

Tree 

age 

(years)

59

60

58

40

49

34

Sediment 

depth 

(cm)

29

27

30

26

27

22

D/A 

(cm/yr)

0.49

.45

.52

.65

.55

.65

Tree 

species

Ash

Ash

Ash

Ash

Ash

Ash

Data Presentation and Analysis 15
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16 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
Table 6. Pre-1950 and post-1950 sedimentation rates at Site 3 

near Momence, III.

[D/A, sediment depth divided by tree age; cm/yr, centimeters per year]

Group

Pre-1950

Post- 1950

Number 

of 

trees

4

2

Age 

range 

(years)

49-60

34-40

Year range 

(years of 

germination)

1933-44

1953-59

D/A 

range 

(cm/yr)

0.45-0.55

0.65

Average 

D/A 

(cm/yr)

0.50

.65

Table 7. Dendrogeomorphic data collected at Site 4 near Momence, III.

[cm, centimeters; cm/yr, centimeters per year; , no data available]

Dbh: Diameter at breast height (1.4 meters).

Inside date: Date of innermost tree ring. Number in parentheses is estimated number of

missed center rings; p indicates that the pith was reached in the core. 

Tree age: Age including minimum number of missed center rings. 

Sediment depth: Net sediment accumulation during lifetime of tree. 

D/A: Sediment depth divided by tree age (net sedimentation rate). 

Tree species: Either ash (Fraxinus) or elm (Ulmus).

Tree 

number

BS1-1

-2

-3

-4

-7

-8

-9

-10

-11

-12

-13

-14

-15

-16

-17

-18

Dbh

12

20

18

12

14

18

28

9

12

4

-

33

14

30

21

17

Inside date

1963 (2-3)

1932(1-2)

1932 (p)

1955 (p)

1941 (p)

1940(1-2)

1927 (2-3)

1917(0-1)

1952 (2-3)

1955 (0-1)

1954 (p)

1934 (p)

1945 (2-3)

1940(1-2)

1935(1-2)

1937(1-2)

Tree 

age 

(years)

32

62

61

38

52

54

68

76

43

38

39

59

50

54

59

57

Sediment 

depth 

(cm)

38

23

13

15

23

25

56

64

40

37

24

26

18

37

51

55

D/A 

(cm/yr)

1.2

.37

.21

.39

.44

.46

.82

.84

.93

.97

.62

.44

.36

.69

.86

.96

Tree 

species

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Table 8. Pre-1950 and post-1950 sedimentation rates at Site 4 near

Momence, III.

[D/A, sediment depth divided by tree age; cm/yr, centimeters per year]

Group

Pre-1 950

Post- 1950

Number 

of 

trees

11

5

Age 

range 

(years)

50-76

32-43

Year range 

(years of 

germination)

1917-43

1951-61

D/A 

range 

(cm/yr)

0.21-0.96

0.40-1.2

Average 

D/A 

(cm/yr)

0.59

.82

Data Presentation and Analysis 17
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18 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
side of the channel. The net sedimentation rate was 

greater during the post-1950 period than during the 

pre-1950 period, similar to Sites 2 and 3.

Site 5, an ash-maple site near a backwater cutoff 

meander, was on the south side of the channel, southeast from Site 4 (fig. 2). Tree ages ranged from 32 to 

78 years, and the sediment depths for the lifetimes 

of the trees ranged from 27 to 62 cm (table 9). The 

data from Site 5 indicate essentially the same net 

sedimentation rate for the pre- and post-1950 periods 

(table 10). A graph of the data (fig. 10) implies a 

linear trend; that is, no shift is present in the data as 

at Site 1.

Site 6 was about 500 m downstream from Site 4. 

Site 6 was an ash-maple site near another backwater

cutoff meander on the south side of the channel 

(fig. 2). Tree ages ranged from 25 to 99 years, and 

sediment depths during the lifetimes of the trees at this 

site ranged from 17 to 61 cm (table 11). Four trees 

sampled here were older than trees sampled at any 

other site. At least four trees at Site 6 pre-dated completion of channelization in Indiana (about 1918).

Because of the number of older trees at Site 6, 

data were summarized by grouping into three age 

groups: pre-1925, 1925-50, and post-1950. The 

youngest age group (post-1950) included only two 

trees. The summarization table (table 12) shows 

the smallest net rate of sediment accumulation for the 

pre-1925 group (0.53 cm/yr), with a greater rate for the 

1925-50 group (0.72 cm/yr), and with the post-1950

Table 9. Dendrogeomorphic data collected at Site 5 near Momence, III.

[cm, centimeters; cm/yr, centimeters per year] 

Dbh: Diameter at breast height (1.4 meters). 

Inside date: Date of innermost tree ring. Number in parentheses is estimated number of

missed center rings; p indicates that the pith was reached in the core. 

Tree age: Age including minimum number of missed center rings. 

Sediment depth: Net sediment accumulation during lifetime of tree. 

D/A: Sediment depth divided by tree age (net sedimentation rate). 

Tree species: Either ash (Fraxinus) or elm (Ulmus).

Tree 

number

BS1E-1

-2

-3

-4

-5

-6

BBS-1

-2

-3

-4

-5

-6

-7

Dbh

18

23

32

40

24

28

32

44

15

18

39

27

52

Inside 

date

1954(0-1)

1937(0-1)

1937 (p)

1939(0-1)

1953 (2-3)

1961 (p)

1954(1-2)

1915 (p)

1937 (p)

1953 (p)

1931(0-1)

1937(0-1)

1918 (p)

Tree 

age 

(years)

39

56

56

54

42

32

40

78

56

40

62

56

75

Sediment 

depth 

(cm)

34

49

48

47

38

27

29

62

42

30

47

41

56

D/A 

(cm/yr)

0.87

.87

.86

.87

.90

.84

.73

.79

.75

.75

.76

.73

.75

Tree 

species

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Table 10. Pre-1950 and post-1950 sedimentation rates at Site 5 

near Momence, III.

[D/A, sediment depth divided by tree age; cm/yr, centimeters per year]

Group

Pre-1950

Post-1950

Number 

of 

trees

8

5

Age 

range 

(years)

54-78

32-42

Year range 

(years of 

germination)

1915-39

1951-61

D/A 

range 

(cm/yr)

0.73-0.87

0.73-0.90

Average 

D/A 

(cm/yr)

0.80

.82

Data Presentation and Analysis 19
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20 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
Table 11. Dendrogeomorphic data collected at Site 6 near Momence, III.

[cm, centimeters; cm/yr, centimeters per year; , no data available]

Dbh: Diameter at breast height (1.4 meters).

Inside date: Date of innermost tree ring. Number in parentheses is estimated number of

missed center rings; p indicates that the pith was reached in the core. 

Tree age: Age including minimum number of missed center rings. 

Sediment depth: Net sediment accumulation during lifetime of tree. 

D/A: Sediment depth divided by tree age (net sedimentation rate). 

Tree species: Either ash (Fraxinus), elm (Ulmus), or oak (Quercus).

Tree 

number

R-l

_2

-3

-4

-5

-6

-7

-10

-12

-13

-14

-15

-16

-17

Dbh

35

-

-

-

-

14

20

25

13

42

28

7

29

20

Inside 

date

1903 (3-5)

1922 (3-5)

1947 (3-5)

1894(p)

1965(1-2)

1938 (p)

1937 (p)

1938(1-2)

1937 (p)

1938(1-2)

1939(1-2)

1970 (2-3)

1910(2-3)

1897 (p)

Tree 

age 

(years)

93

74

49

99

29

55

56

56

56

56

55

25

85

96

Sediment 

depth 

(cm)

53

38

32

55

34

24

61

40

37

43

40

17

50

42

D/A 

(cm/yr)

0.57

.51

.65

.56

1.2

.44

1.1

.71

.66

.77

.73

.68

.59

.44

Tree 

species

Ash

Ash

Ash

Ash

Oak

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Ash

Table 12. Pre-1925, 1925-50, and post-1950 sedimentation rates at Site 6 

near Momence, III.

[D/A, sediment depth divided by tree age; cm/yr, centimeters per year]

Group

Pre-1925

1925-50

Post- 1950

Number 

of 

trees

5

7

2

Age 

range 

(years)

74-99

49-56

25-29

Year range 

(years of 

germination)

1894-19

1937-44

1964-68

D/A 

range 

(cm/yr)

0.44-0.59

0.44-1.1

0.68-1.2

Average 

D/A 

(cm/yr)

0.53

.72

.93

group having the greatest rate (0.93 cm/yr). The 

pre-1925 period probably included much of the channelization activity in Indiana. Sediment deposition 

during that time period might have been expected to 

have been exceptionally large during channel construction but appears to have been just the opposite. 

A graph of the data from Site 6 is shown in figure 11.

Interpretation of the Data

The net sedimentation rate for the pre-1950 

period at Site 1 (0.34 cm/yr) is about 3 times smaller 

than for the post-1950 period (0.93 cm/yr) (table 13), 

indicating that either little or no deposition resulted 

before 1950 or there has been erosion of material from

Interpretation of the Data 21
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22 Oendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
Table 13. Summary of net sedimentation rates at data-collection sites 

near Momence, III.

[D/A, sediment depth divided by tree age; Average D/A, average of D/A of every tree at 

that site; Ages, range of tree ages]

Site

1

2

3

4

5

6 

6

Ages

54-69

44-47

49-60

50-76

54-78

49-56 

74-99

Pre-1950

Number 

of trees

4

3

4

11

8

7 

5

Average 

D/A

0.34

.42

.50

.59

.80

.72 

.53

Ages

9-40

28-40

34-40

32-43

32-42

25-29

Post-1950

Number 

of trees

19

4

2

5

5

2

Average 

D/A

0.93

.54

.65

.82

.82

.93

Average of all D/A 0.59 0.75

the site. Large, relatively old elm trees on the natural 

levee indicates that the levee was present before 1950. 

It is likely sediment was deposited before 1950, but 

much of the sediment deposited between the time the 

older trees were established and 1950 appears to have 

been eroded. Active erosional features on the levee 

at Site 1 also suggest the possibility that erosion might 

have altered depths of sediment deposits.

The data collected at Sites 2 and 3 also showed 

an increase in net sedimentation rates from before 

1950 to after 1950 (table 13). The net sedimentation 

rate of the earlier period was smaller, indicating the 

possibility of sediment loss by erosion, but no active 

erosional features were present. Because no such 

features were present and because the area has 

remained essentially unchanged over the past several 

decades, it is assumed that loss of sediment by erosion 

was minimal.

The Kankakee River upstream from Momence 

to the State line has very little gradient and inundates 

the Momence Wetland when it overflows its banks. 

Flow velocities on the relatively wide flood plain of 

the river, except near the channel, are assumed to be 

very low. The absence of active erosional features 

supports this assumption.

Data from Sites 4 and 6 (table 13) also indicated 

increasing net sedimentation rates during the lifetime 

of the trees. Data at Site 5 (table 13) also indicated 

an increase in net sedimentation rate from pre- to post1950, but not such a marked increase as other sites.

One factor that could have caused a change of 

the sedimentation rate is a change in streamflow. An 

increase in streamflow usually will cause an increase

in sediment transport in a stream. Also, it is assumed 

in the dendrogeomorphic method that if an area is 

inundated more frequently, more sediment will settle 

on the flood plain, resulting in greater sedimentation 

rates. Bhowmik and others (1980, figs. 18 and 21) 

used mean annual discharge data from the USGS 

streamflow-gaging stations to point out that streamflow in the Kankakee River Basin had been increasing 

for perhaps the last 50 years (fig. 12). Their analysis 

was repeated for this study with data through 1992. 

The increases in streamflow have continued since the 

1980 study (fig. 12). The increasing streamflow does 

not seem to be unique to the Kankakee River Basin. 

Blanchard and Schmidt (in press) reported "significant 

upward trends" in streamflow at 23 of 25 stations in 

the upper Illinois River Basin during 1978-86. The 

25 stations represented drainage areas with urban, 

agricultural, and mixed land uses. Many factors can 

affect streamflow, such as changes in channel geometry (for example, straightening or dredging of a channel and draining of a wetland); quantity, duration, and 

intensity of rainfall; and changes in land-use practices.

Precipitation data through 1992 were obtained 

(National Oceanic and Atmospheric Administration, 

1921-92) at two rain-gaging stations in the upper 

Kankakee River Basin-at Wheatfield and Plymouth, 

Ind. (fig. 1). Data from these stations are shown in 

figures 13 and 14. The precipitation data show an 

upward trend since the early 1900's and provide at 

least one explanation for the observed increases in 

streamflow.

Less likely causes of the observed increases 

in net sedimentation rates are erosion and compaction, 

which might have reduced the actual sediment depth.

Interpretation of the Data 23
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26 Oendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
Erosion during earlier years and little or none in more 

recent years would have resulted in increasing net 

sedimentation rates, but no evidence indicated that 

erosion was a cause. Soil compaction depends on 

how easily material making up the soil may be consolidated. Soils of the study area are described as 

Gilford fine sandy loam and are grouped in the coarsegrained soil classes SM and SC in the Unified Soil 

Classification System (U.S. Department of Agriculture, 1990). This type of soil is not easily compacted.

A study in the Momence Wetland, about 10 km 

downstream, showed that study area was flooded at a 

discharge of around 113 m3/s (Mitsch and Rust, 1984). 

USGS personnel noted on several occasions that the 

data-collection sites were inundated at a lower discharge (around 85 m3/s). The estimated period of 

inundation of the study area at 85 and 113 m3/s is 

shown in table 14. This inundation period was 

calculated for different time periods and shows that the 

area is more subject to inundation in recent years than 

about 50 years ago.

Dendrogeomorphic determinations of sediment 

depth as described in this report are primarily based on 

sedimentation in backwater meanders. A major 

assumption of this study was that sedimentation on the 

flood plain has some association with sand movement 

in the channel. The relation between sand movement 

in the channel and sediment deposition on the flood 

plain, however, has not been determined. In order for 

the rate of sediment deposition in the backwater areas 

to reflect the rate of sediment transport in the river 

channel, sediment at the sites around the meanders 

must be from the channel and not from other sources.

Other than the river channel, two possible sources of 

sediment in the backwater meanders are (1) reworked 

bank material from lateral movement (meandering) of 

the channel, and (2) locally eroded material.

Reworking of former bank material is unlikely. 

Comparison of the most recent 7'/2-minute topographic 

map (1973) of the area with older maps (15-minute 

topographic map, 1924) and with present channel configuration indicates that the main channel in the study 

area has not moved appreciably since channelization 

in Indiana was completed around 1918. Further, the 

number and size of large canopy trees between the 

backwater cutoff meanders and the present channel 

also indicate that the channel has remained in its 

present location for at least 30 years. It does not 

appear that sediment deposits around the backwater 

meanders sampled in this study include sediment from 

lateral movement of the channel.

It is unlikely that the sediments deposited in the 

study area were eroded from local areas. The area 

between State Highway 114 and the data-collection 

sites (fig. 2) is forested and has remained forested 

because it is too poorly drained to be suitable for 

cultivation. The sediment deposits in the study area 

completely encircle the cutoff meanders but do not 

extend between the meanders and State Highway 114. 

It is unlikely that sediment in the study area was 

transported from farmland across the poorly drained, 

heavily vegetated area south of the river. Elimination 

of these two possible sources would indicate that sediments associated with the cutoff meanders are material 

that was transported in the river channel; that is, by 

floodwaters of the Kankakee River.

Table 14. Estimated period of inundation of data-collection sites along the Kankakee 

River near Momence, III.

[m3/s, cubic meters per second. Data for the streamflow-gaging station at Kankakee River at Momence, 111. 

(05520500)]

Assuming 85 m3/s 

will inundate sites

Assuming 113 m3/s 

will inundate sites

Time 

period

1905-92

1905-50

1950-92

1980-92

Percent of time 

sites are 

inundated

21

17

25

29

Number of days 

per year sites 

are inundated

77

62

91

106

Percent of time 

sites are 

inundated

12

8

15

19

Number of days 

per year sites 

are inundated

44

29

55

70

Interpretation of the Data 27
SUMMARY AND CONCLUSIONS

Past sedimentation rates were estimated for 

six sites along the Kankakee River near Momence, 111., 

utilizing a dendrogeomorphic technique. Five sites 

were areas of sediment deposition near backwater 

cutoff meanders containing mostly ash and maple 

trees. The sixth site was on a natural sand levee 

on an inside bend of the channel containing mostly 

elm and maple trees. Net sedimentation rate at 

each tree sampled was estimated as the total depth 

of sediment accumulated (depth of original lateral root 

burial) divided by the age of the tree. Examination of 

root burial depth of trees of a variety of ages permitted 

estimation of net sedimentation rates before and after 

1950. The following is a summary of the analysis of 

the dendrogeomorphic data:

1. Dendrogeomorphic evidence indicated a 

greater net sedimentation rate for trees established 

after 1950 compared to trees established before 1950, 

at all but one site along the upper reaches of the 

Kankakee River in Illinois. No data indicated that 

the net sedimentation rate of the trees established after 

1950 was less than the rate of the trees established 

before 1950.

2. Possible explanations for apparent 

increased sedimentation rates since 1950 include 

erosion, soil compaction, and increased streamflow. 

No evidence of erosion was observed, except at Site 1, 

indicating that effects from erosion were minimal. 

Data indicated a major erosional event at Site 1 that 

might have resulted from a flood in 1950. Soils at all 

the study sites are not easily compacted, indicating 

that effects of compaction were minimal. Streamflow at four gaging stations in the Kankakee River 

Basin has increased over the period of record of each 

station, possibly resulting in increased sedimentation. 

The degree to which increased streamflow has caused 

increased sedimentation is not known. Not enough 

data were collected to determine if sedimentation is 

increasing at a rate commensurate with streamflow 

increases.

REFERENCES CITED

Bhowmik, N.G., and Bogner, W.C., 1981, Sediment 

transport and hydraulics of flow in the Kankakee 

River, Illinois-Phase II: Illinois State Water 

Survey Contract Report 282, 67 p.

Bhowmik, N.G., Bonini, A.P., Bogner, W.C., and

Byrne, W.C., 1980, Hydraulics of flow and sediment 

transport in the Kankakee River in Illinois: Illinois 

State Water Survey, Report of Investigation 98, 181 p.

Blanchard, S.F., and Schmidt, A.R., in press, Water-quality 

assessment of the upper Illinois River Basin in Illinois, 

Indiana, and Wisconsin Analysis of available surfacewater-quality data through 1986: U.S. Geological 

Survey Open-File Report 94-30.

Gleason, H.A., 1952, The illustrated flora of the

northeastern United States and adjacent Canada: 

The New York Botanical Garden, N.Y., in three vols., 

482 p., 655 p., and 595 p.

Gross, D.L., and Berg, R.C., 1981, Geology of the 

Kankakee River system in Kankakee County, 

Illinois: Illinois Institute of Natural Resources, 

State Geological Survey Division, Environmental 

Geology Notes 92, 80 p.

Guilkey, PC., 1957, Silvical characteristics of American 

elm (Ulmus americana): Lake States Forest 

Experimentation Station, St. Paul, Minn., 

Paper no. 54, 19 p.

Houde, M.J., and Klasey, John, 1968, Of the people, a 

history of Kankakee County: Chicago, 111., The 

General Printing Company, 436 p.

Hupp, C.R., and Bazemore, D.E., 1993, Temporal and 

spatial patterns of wetland sedimentation, West 

Tennessee: Journal of Hydrology, v. 141, p. 64.

Hupp, C.R., and Morris, E.E., 1990, A dendrogeomorphic 

approach to measurement of sedimentation in a 

forested wetland, Black Swamp, Arkansas: 

Wetlands, v. 10, p. 107-124.

Hupp, C.R., Woodside, M.D., and Yanosky, T.M., 1993, 

Sediment and trace element trapping in a forested 

wetland, Chickahominy River, Virginia: Wetlands, 

v. 13, p. 95-104.

Ivens, J.L., Bhowmik, N.G., Brigham, A.R., and

Gross, D.L., 1981, The Kankakee River yesterday 

and today: Illinois State Water Survey 

Miscellaneous Publication 60, 24 p.

Leopold, L.B., Wolman, M.G., and Miller, J.P, 1964,

Fluvial processes in geomorphology: San Francisco, 

Calif., W.H. Freeman and Co., 522 p.

Little, E.L., Jr., 1979, Checklist of United States trees: 

Forest Service, U.S. Department of Agriculture, 

Agricultural Handbook 541, 375 p.

Mitsch, W.J., and Rust, W.G., 1984, Tree growth responses 

to flooding in a bottomland forest in northeastern 

Illinois: Forest Science, v. 30, p. 499-510.

National Oceanic and Atmospheric Administration, 

1921-92, Climatological data annual summaries, 

Indiana: National Climatic Data Center, Asheville, 

N.C. (published annually).

28 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois
Phipps, R.L., 1985, Collecting, preparing, crossdating and 

measuring tree increment cores: U.S. Geological 

Survey Water-Resources Investigations Report 

85-4148, 48 p.

Sigafoos, R.S., 1964, Botanical evidence of floods and 

flood-plain deposition: U.S. Geological Survey 

Professional Paper 485-A, p. A1-A35.

U.S. Department of Agriculture, 1990, Soil survey of 

Kankakee County, Illinois: 182 p.

U.S. Geological Survey, 1964, Compilation of records 

of surface waters of the United States, October 1950- 

September 1960: U.S. Geological Survey WaterSupply Paper 1728, 576 p.

U.S. House of Representatives, 1916, Kankakee River, 

Illinois and Indiana: Letter from the Secretary of 

War, 64th Congress, First Session, Document 931.

 1931, Kankakee River, Illinois and Indiana: 

Letter from the Secretary of War, 71st Congress, 

Third Session, Document 784.

Wright, J.W, 1959, Silvical characteristics of green ash 

(Fraxinus pennsylvanica): Upper Darby, Penn., 

Northeastern Forest Experimentation Station, Paper 

no. 126, 18 p.

References Cited 29
GLOSSARY

Active erosional feature. A characteristic of an area that 

seems to be presently eroding; for example, a gully that 

appears freshly cut.

Adventitious roots. Roots that sprout from, and at right 

angles to, a root or stem. Adventitious roots may 

develop on buried stem wood.

Backwater. A general term referring to standing water 

that is away from the moving water of the stream 

but whose level is affected by that of the stream. 

Backwater areas in the Momence Wetland contain 

the old cutoff meanders.

Bottomland. An informal term that refers to the flat land 

on either side of a stream. It usually includes the 

flood plain and surrounding area.

Channelization. Modification of a stream to confine it to 

an artificial (usually straight) ditch or channel.

Cutoff meander. See meander.

D/A. Sedimentation rate; that is, sediment depth divided by 

tree age.

Dendrochronology. The science that is concerned with 

the study of tree rings for the information that may be 

obtained from them.

Dendrogeomorphology. A branch of science that combines dendrochronology and geomorphology. 

Dendrogeomorphology involves the use of tree rings to 

obtain information of hydrologic interest.

Depositional area. An area in which material is deposited, such as an area of sediment deposition.

Diffuse-porous. Refers to a type of wood. Trees in the 

Momence Wetland that have diffuse-porous wood 

include such tree species as silver maple, willow, and 

sycamore.

Dissecting microscope. A microscope specially designed 

to provide a wide view at low power (magnification).

Equilibrium. With reference to a river, equilibrium

implies that the geomorphic and hydrologic processes 

that form the river are in balance. When in equilibrium the sedimentation rate should be neither increasing nor decreasing.

Flood plain. A plain (flat surface) along either side of a 

river through which, over many centuries, the river will 

meander. Leopold and others, 1964, defined the flood 

plain as the surface that is flooded, on the average, 

about once every 1.5 years. By this definition, a 

riverine wetland, such as the Momence Wetland, is 

usually flooded at least once every year and occupies a 

surface lower than the flood plain; however, throughout the report this lower surface is referred to as bottomland or flood plain.

Hydrology. The science dealing with the nature and properties of water.

Increment core. A small pencil-shaped core that may be 

taken from a tree with an increment borer. Tree rings 

may be viewed on increment cores. Increment cores 

thus provide a means by which tree ages may be determined while doing little or no damage to the tree.

Lateral roots. Roots that grow more-or-less horizontally, 

or laterally, from a vertical axis or stem.

Marsh. Wetland. Sometimes a marsh is considered as a 

type of wetland that contains grass and few or no trees. 

The terms marsh and wetland are used interchangeably 

in this report.

Meander. A bend in the river. As a meander becomes 

more extreme, it has an increased chance of being cut 

off from the river. A small cutoff meander may be 

referred to as a slough. Large cutoff meanders are 

often called oxbows or oxbow lakes.

Original lateral roots. Lateral roots that develop just 

below the soil surface on which the seedling became 

established.

Riverine wetland. A wetland along a river.

Root crown. The base of the tree trunk from which lateral 

roots arise. The root crown is characteristically wider 

than the tree trunk above it.

Sediment. Gravel, sand, silt, and clay that may be moved 

by river water.

Sedimentation. The process of sediment accumulation at 

any particular location.

Sedimentation rate. Sediment deposited per unit time. 

In this report, sedimentation rate is calculated as 

sediment depth divided by tree age, and is referred to 

as D/A.

Slough. A very wet area that usually contains at least 

some standing water. As used herein a slough is 

synonymous with backwater and cutoff meander.

Suspended sediment. Sediment that is small enough to 

be held in suspension by the upward component of turbulence in moving water. Generally, particles less 

than 0.062 mm diameter are considered small enough 

to be constantly suspended and moved with the water 

column.

Tap root. A root that grows vertically along the main axis 

of the tree.

Tree ring. An annual growth layer of a woody plant. 

When viewed in cross section, such as on a stump top, 

the annual growth layer appears as a ring.

Water table. In a nonconfining soil, such as that of a 

flood plain, it is the level at which water stands in a 

well. Though usually below the surface of upland 

soils, the water table of a wetland may often be above 

the surface.

Wetland. A low, wet area that usually contains some 

standing water. The water table in a wetland is close 

to the surface most of the time. A wetland is expected 

to be inundated for at least a short time every year.

30 Dendrogeomorphic Estimate of Changes in Sedimentation Rate Along the Kankakee River Near Momence, Illinois