r) :7

THE RELATIONSHIPS BETWEEN MORPHOSTRATIGRAPHY.‘
ROCK STRATl’GRAPHY, AND ASPECTS or m FABRIC "
m CENTRAL ILLINOIS“

Thesis for the Degree of Ph. D.
MICHIGAN STATE UNIVERSITY
DAVID AlAN CASTI‘LLON
' A 1972

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This is to certify that the

thesis entitled

The Relationships Between Morphostratigraphy
Rock Stratigraphy, and Aspects of Till Fabric
In Central Illinois

presented by

David Allan Castillon

has been accepted towards fulfillment
of the requirements for

Ph . D . degree in Geo graphL

f/V/Jz/(A fies,

Major professor

Date November 3, 1972 ’

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SUPPLEMENTARY
MATERIAL

IN BACK OF BOOK

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ABSTRACT

THE RELATIONSHIPS BETWEEN MORPHOSTRATIGRAPHY,
ROCK STRATIGRAPHY, AND ASPECTS OF TILL FABRIC

IN CENTRAL ILLINOIS

By
David Alan Castillon

This thesis is concerned with the relationship between
selected morphostratigraphic units and aspects of rock
stratigraphy including pebble orientation in central Illinois.
Investigations were made to determine the nature of the areal
relationships between rock stratigraphy and morphostratigraphy
of the Woodfordian end moraines in central Illinois. Included
in these investigations was an analysis of long-axis pebble
orientation of the till fabric. The nature of the sedimentary
contact zone deposited by two lobes of Woodfordian glacial
ice was studied to determine if morphostratigraphic units in
an interlobate area could be delineated by the use of pebble
orientation data or rock stratigraphy. Analysis of the pebble
lithology of elongate stones was made to determine if a
discernible difference in lithologic composition exists
between delineated morphostratigraphic units or between

delineated rock-stratigraphic units.

L‘iSL’Q’.

David Alan Castillon

Thirty-eight analysis sites within the till of the
Bloomington, Champaign, Eureka, and Normal Morphostratigraphic
Units were selected. At each of these sites a random
fifty-pebble sample was examined by established methods of
till-fabric analysis. The pebbles' long-axis orientation was
measured to the nearest five degrees and the dip strength was
recorded. These same pebbles were classified lithologically
in the laboratory. A sample of the till matrix surrounding
the fifty pebbles was collected and analyzed by the laboratory
of the Illinois State Geological Survey providing data on
grain size, clay mineral composition, and carbonate content.
Data on the color of the till matrix were provided by the
author. These data were used to identify and correlate rock
stratigraphic units.

The findings of this study indicate that the Eureka and
Normal Morphostratigraphic Units should be mapped as a single
unit identified as the Eureka-Normal Moraine (Drift). The
physical characteristics of the till within the Eureka-Normal
Moraine (Drift) indicate that this morphostratigraphic unit
has a single rock-stratigraphic unit surface till which can
be correlated with the Malden Till of the Wedron Formation.
Pebble-orientation data from analysis sites along the trend
of the Eureka-Normal Moraine (Drift) reveal that the long
axis of elongate pebbles within the Malden Till prefer a
perpendicular alignment to the trend of the moraine. These

orientations indicate a Lake Michigan Lobe source. Pebble

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David Alan Castillon
lithology data show that a lower percentage of crystalline
pebbles and a larger percentage of carbonate pebbles are embedded
in this till than were found in tills from the other morpho-
stratigraphic units of this study.

The data from analysis sites within the till of the
Champaign Moraine (Drift) indicate that this morphostratigraphic
unit is well defined topographically and that the surface till
of this unit can be correlated with the Snider Till of the
Wedron Formation. This same rock-stratigraphic unit was
correlated with the till on the eastern flank of the inter-
lobate region. This portion of the interlobate region adjoins
and can be associated with the Champaign Moraine (Drift) of
this study. The long-axis pebble orientations of the Champaign
Moraine (Drift) tend to be orthogonal to the trend of the
morphostratigraphic unit outside of the interlobate, then
become parallel to the trend of the landform in the associated
interlobate region. An Brie Lobe source can be postulated
for the Snider Till from these orientation findings. Pebble
lithology data from the Champaign Moraine (Drift) and
associated interlobate area indicate that pebbles within till
from an Brie Lobe source have approximately 9 per cent fewer
carbonate pebbles when compared with pebble lithology data
from the Eureka-Normal Moraine (Drift) which has a Lake Michigan
Lobe source.

The findings of this study reveal that the Bloomington

Moraine (Drift) is very complex. Three distinct surface

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David Alan Castillon
tills within this morphostratigraphic unit can be delineated:
the Tiskilwa, Malden, and Shamrock Till Members. The latter was
named and defined in this study. As was the case with the other
units investigated in this study, the long axis of pebbles
embedded in these tills preferred a perpendicular alignment to
the trend of the moraine outside of the interlobate area. In
the interlobate region associated with the Malden Till of the
Bloomington Moraine (Drift) pebble-orientation data once again
reveal a strong tendency for pebbles to align themselves
parallel to the trend of the landform.

Because the relationships between morphostratigraphy,
rock stratigraphy, and till fabric did not complement one
another within the area of the Bloomington.Moraine (Drift)
as they did on the other units of this study, an alternate
interpretation of the morphostratigraphy was investigated.
An alternate interpretation must account for three distinct
rook-stratigraphic units and also account for an ice source
region that will explain its fabric. An analysis of the
topography of the Bloomington Moraine (Drift) indicates that
it is not necessarily one morphostratigraphic unit. Instead,
it may represent a situation where three units of different
age converge on one another. The oldest unit identified by
the presence of Tiskilwa Till, which is the surface till west
of Bloomington, Illinois, and exists over a wide area in the
subsurface, was deposited by an ice advance from the north.

The Shamrock Till, whose fabric orientations suggest it was

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David Alan Castillon

deposited by a western advance, possibly of the Erie Lobe,
was deposited and overlies the Tiskilwa Till. A third and
younger till unit which is the surface till within the moraine
everywhere east of the Kickapoo Creek Valley and also the
surface till on a part of the proximal slopes to the west of
this stream was deposited contemporaneously with the Snider Till
of the Champaign Moraine (Drift) forming the interlobate
moraine. The time-stratigraphic correlation of Malden and
Snider Tills suggested by the fabric orientations in the inter-
lobate region, which are parallel to the ice-contact zone,
and the similar physical characteristics of these two till
members suggest that the landform associated with this region
be named the Champaign-Bloomington Interlobate Mbraine (Drift).

0f general interest to the area of glacial geomorphology
is the finding of this study that morphostratigraphic units
exist and can be useful geomorphically when sedimentary

parameter data complement the landform unit.

 

in

THE RELATIONSHIPS BETWEEN MORPHOSTRATIGRAPHY,
ROCK STRATIGRAPHY, AND ASPECTS OF TILL FABRIC
IN CENTRAL ILLINOIS

BY

David Alan Castillon

A THESIS

Submitted to
Michigan State University
in partial fulfillment of the requirements

for the degree of

DOCTOR OF PHILOSOPHY

Department of Geography

1972

Dedicated to
Joanne

Cindy, Kim, Linda, Laura,
and David Alan II

ii

ACKNOWLEDGMENTS

I wish to express my thanks to my committee, which was

chaired by Dr. H. A. Winters and consisted of Dr. J. R. Harman,
Dr. G. Higgs, and Dr. H. D. Poth; to the Illinois State
Geological Survey and in particular to Dr. C. Collinson,

P. Perkins, Dr. H. D. Glass, Dr. H. B. Willman,

Dr. J. P. Kempton, Dr. D. L. Gross, and Dr. J. C. Frye of the
Illinois State Geological Survey for their help and assistance;
to my typist Sandy Aper for a fine job; and finally a special
thanks to my wife Joanne, my daughters Cindy, Kim, Linda,

and Laura, and my son David Alan II for their patience,
understanding, and encouragement during the writing of this

thesis.

iii

iater.

'1...
«after

"A .
‘APter

TABLE OF CONTENTS

Chapter 1 INTRODUCTION
Statement of Problem
Study Area
Morphostratigraphy
Rock Stratigraphy
Till Fabric
Till Matrix Composition
Data and Analysis Sites
Justification for the Study

Chapter 2 FIELD WORK AND LABORATORY ANALYSIS
Selection of the Study Area
Introduction
Study Area
Selection of Analysis Sites
Introduction
Analysis Sites
Field Technique
Introduction
Till Fabric Analysis
Laboratory Analysis of Pebbles
Introduction
Pebble Shape
Pebble Lithology
Laboratory Analysis of Till Matrix
Introduction
Grain Size Analysis
X-ray Diffraction Analysis
Color Analysis

Chapter 3 CHARACTERISTICS OF THE EUREKA-NORMAL
MORPHOSTRATIGRAPHIC UNIT
Introduction
Physical Characteristics of the
Till Matrix
Characteristics of Till Pebbles
Introduction
Till Pebble Orientation
Till Pebble Lithology
Congerville Section
Conclusions

iv

45
45

47
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Chapter 4

Chapter 5

Chapter 6

CHARACTERISTICS OF THE CHAMPAIGN
MORPHOSTRATIGRAPHIC UNIT AND ASSOCIATED
INTERLOBATE AREA
Introduction
Physical Characteristics of the
Till Matrix
Characteristics of Till Pebbles
Introduction
Till Pebble Orientation
Till Pebble Lithology
Conclusions

CHARACTERISTICS OF THE BLOOMINGTON
MORPHOSTRATIGRAPHIC UNIT AND ASSOCIATED
INTERLOBATE AREA
Introduction
Physical Characteristics of the
Till Matrix
Characteristics of Till Pebbles
Introduction
Till Pebble Orientation
Till Pebble Lithology
Shamrock Section
Conclusions

CONCLUSIONS AND IMPLICATIONS
Introduction
General Implications
An Alternate Interpretation of the
Morphostratigraphy in Central Illinois
Conclusions on the Glacial Geomorphology
of Central Illinois
Suggestions for Future Investigations

LIST OF REFERENCES

APPENDIX

Page

65
65

67
72
72
72
74
76

77
77

79
86
86
87
91
94
96

97
97
97
100

104
104

106

111

Table

LIST OF TABLES

Title

Physical Characteristics of the Till Matrix--
Eureka-Normal Till

Pebble Lithology--Eureka-Normal Till

Physical Characteristics of the Congerville
Section Samples

Physical Characteristics of the Till Matrix--
Champaign Till and Associated Interlobate Till

Pebble Lithology--Champaign Till and
Associated Interlobate Till

Physical Characteristics of the Till Matrix--
Bloomington Till and Associated Interlobate
Till

Pebble Lithology--Bloomington Till and
Associated Interlobate Till

Page

50

59

61

75

82

92

Figure

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10
11
12
13
14

15

LIST OF FIGURES

Title Page

Map of Illinois illustrating study area 3
Stratigraphic classification of the Pleistocene
deposits of Illinois 6
Woodfordian lobes and sublobes in Illinois 8
Woodfordian.Moraines of Illinois in pocket
Areal distribution of till formations and
members in Illinois 10
Correlated till members and till units l3
Morphostratigraphic units of the study area
with general location of analysis sites 20
Examples of analysis sites

Pipeline trench 24

Borrow pit 24

Roadcut with dig 26

Close up of dig illustrating dip measurement 26
Interlobate map 29
Slope development classification 30
Random sample of fifty pebbles 33
Representative pebble shape categories 33
Peoria 1:250,000 tOpographic map in pocket
Relationship between morphostratigraphy
and pebble orientation in pocket
McLean County drill boring locations 85

vii

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20

22

23

32

33

35

36

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39

Figure
16

17

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30
31
32
33

35
36
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Relationships between.morphostratigraphic
units, rock stratigraphic units, and

Title

ice flow in the study area

An alternate interpretation of the
morphostratigraphy of Central Illinois

Data
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Chapter 1
INTRODUCTION

Statement of Problem

This thesis is concerned with the relationships between
selected morphostratigraphic units and aspects of rock
stratigraphy including pebble orientation in central Illinois.l
Several specific matters, listed below, were investigated in
an effort to determine these relationships. (1) The nature
of the relationship between rock stratigraphy and morphostrati-
graphy of the‘Woodfordian end moraines in central Illinois was
investigated. (2) The nature of the relationship between the
pebble orientations of the till fabric and morphostratigraphy
of the‘Woodfordian end moraines in central Illinois was
investigated. (3) Investigations of the contact zone between
two glacial lobes of the Woodfordian glacial ice were made to
determine if morphostratigraphic units in an interlobate area
could be delineated by the use of pebble-orientation data
or rock stratigraphy. And (4) investigations were made to
determine if a discernible difference in pebble lithology of
the collected orientated stones exists between delineated
morphostratigraphic units, or between delineated rock-

stratigraphic units.

 

1The study area is defined on page two and illustrated
in Figure 1.

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Study Area

 

The study area selected in central Illinois contains one
of the best examples in North America of arcuate-lobate end
moraines with good t0pographic expression that merge into what
appears to be an interlobate area. The study area has an
approximate east-west extent of 40 miles (73 kilometers) and
north-south extent of 30 miles (48 kilometers), and includes
parts of Champaign, Ford, McLean, Piatt, and.Woodford Counties
in Illinois. The study area is delineated in Figure l, a
map of Illinois.

The literature describing various aspects of all or part
of this area is extensive. An early work, very comprehensive
for its time and entitled "The Illinois Glacial Lobe," was
written in 1899 by Frank Leverett. This monograph describes
the Pleistocene landforms of the state of Illinois and has
served since its publication as a primary reference for glacial
geology studies in the state. Leverett's interpretation of the
glacial landforms of the study area was modified only slightly
during the first thirty years following publication. He revised
some of his interpretations in 1929 and again in 1932. These
revisions included minor changes in both the delineation of
moraines (Leverett, 1932) and the interpretation and terminology
regarding substages of the Wisconsin glacial stage (Leverett,
1929). From 1932 to the present, changes in the interpretation

of the Wisconsin glacial stage have continued. Two of the more

 

 

 

 

 

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important works concerned with the chronology of the Wisconsin
glacial stage in Illinois were made by Leighton (1958) and Frye
and Willman (1960).2

Many other publications describing various characteristics
of the Wisconsinan glacial drift of Illinois were published in
the 1960's. To cite a few of the more important works: Frye,
Glass, andHWillman (1962) published a study on the stratigraphy
and mineralogy of the Wisconsinan loess; Willman, Glass, and
Frye (1963, 1966) wrote on the mineralogy and weathering profiles
of glacial till; and Piskin and Bergstrom (1967) described the
thickness and Character of the glacial drift of Illinois.

TWO recent publications describing the study area were
written by Willman and Frye (1970) and Kempton, DuMontelle,
and Glass (1971). The former, Bulletin 94 of the Illinois
State Geological Survey entitled "Pleistocene Stratigraphy of
Illinois," is general in nature and covers the entire state
whereas the latter is specific and focuses on till units in
McLean County. ‘

Bulletin 94 is useful because Willman and Frye review
the principles of stratigraphic classification for Pleistocene
deposits. Four different types of stratigraphy may be
recognized: (1) time stratigraphy, (2) morphostratigraphy,
(3) rook stratigraphy, and (4) soil stratigraphy. The study
area for this thesis is a part of the Woodfordian time

 

2Hereafter in this study the term "Wisconsinan" will be
used for‘Wisconsin when referring to the glacial stage as
suggested by Frye and.Wi11man (1960).

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stratigraphic unit, the morphostratigraphic units broadly
defined by the Peoria Sublobe of the Lake Michigan Lobe and
the Decatur Sublobe of the Erie Lobe, the Wedron Formation
rook—stratigraphic unit, and the Jules Soil soil-stratigraphic
unit (see Figure 2). This study is concerned with certain
relationships between morphostratigraphy and rook stratigraphy.
The Kempton, DuMontelle, and Glass (1971) work on the
stratigraphy of‘Woodfordian tills in MCLean County is useful
because it defines five till units, three of which are surface

tills in the study area of this thesis.

Morphostratigraphy

A morphostratigraphic unit is defined "as a body of rock

 

that is identified primarily from the surface form it displays;
it may or may not be distinctive lithologically from contiguous
units; it may or may not transgress time throughout its extent"
(Frye and.Willman, 1960, 1962). Morphostratigraphic units

were proposed in an effort to explain the relationship and
significance of tapographic forms to rock, soil, and time-
stratigraphic units. The term "Drift" is attached to a named
morphostratigraphic unit and is used to connote the deposit

of glacial till and outwash associated with a moraine and
traceable from it into the ground moraine, outwash apron, and
beneath younger drifts (Willman and Frye, 1970). In this study
the term "Moraine" will be retained to include the landform
which is discernible by its topographic expression and the

term "Drift" when included in parentheses following Moraine

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Figure 2 Stratigraphic classification of the Pleistocene

deposits of Illinois (after Willman and Frye,

1970)

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is interpreted to be at least partially representative of the
morphostratigraphic unit as defined by Willman and Frye (1970).
During the Woodfordian Substage two lobes of glacial ice
covered approximately one-third of the northeastern sector of
the state of Illinois (see Figure 3). The Brie Lobe had only
one sublobe in Illinois called the Decatur Sublobe (Frye and
Willman, 1970). The Lake Michigan Lobe had six sublobes (Frye
and Willman, 1970). This study is concerned with some of the
deposits of both the Peoria Sublobe of the Lake Michigan Lobe
and the Decatur Sublobe of the Erie Lobe. These two subldbes
deposited a sequence of Drifts that form the basis of the
morphostratigraphy of the study area (Frye and Willman, 1970).
The map entitled "Woodfordian Moraines of Illinois" (see
Figure 4, in pocket) is included in this dissertation by
permission of the Illinois State Geological Survey and shows
all mapped.Woodfordian morphostratigraphic units in the state.
The individual morphostratigraphic units defined as Drifts
by Willman and Frye (1970) and selected for investigation in
this study are based on part of the Bloomington and Eureka
Moraines and all of the Normal Moraine of the Peoria Sublobe
and part of the Champaign Moraine of the Decatur Sublobe. The
drifts of this study from the Peoria Sublobe merge with the
drift of the Decatur Sublobe to form the interlobate area

(see Figure 4, in pocket).

 

 

  
  

H0
"b. o 0
u:
m
o 20 nuts 00 so 3
II: _

E 1 2
o m carats .0 J I 1 g

L . .
Princeton ‘ 0 'e' ?"
Sublobe “ Sublobe cf)
22
m
r x
4
\. \ ._l

. fx‘,
‘ Peoria Sublobe I, ‘“‘"

, I '

ERIE LOBE

' Decatur Su blobe

 

Figure 3 Woodfordian lobes and sublobes in Illinois
(after Willman and Frye, 1970)

 

' ~
At.

.
,ic-

‘ l
1“. I
«i. I

‘ra,
-|l!

'Vod1
-

:‘QH.

”owe:

a“.

'V-

‘:s 1

 

9

Rock Stratigraphy

 

The American Commission on Stratigraphic Nomenclature
Code (1961, page 649) defines a rock-stratigraphic unit as
follows:

A rock-stratigraphic unit is a subdivision of

the rocks in the earth's crust distinguished and

delimited on the basis of lithologic characteris-

tics....Rock-stratigraphic units are recognized and
defined by observable physical features rather than

by inferred geologic history.

The study area for this thesis lies entirely in the rock-
stratigraphic unit named the‘Wedron Formation (see Figure 5).
The Wedron Formation consists of glacial tills, outwash sands
and gravels associated with the glacial tills, and silt
deposited in Illinois during the Woodfordian Substage of the
Mfisconsinan Stage (Frye et al., 1968; Willman and Frye, 1970).
The formation is bounded below by the Morton Loess or older
deposits and above by the Richland Loess (Frye et al., 1968).
Its type section is the Wedron Section, Wedron Silica Company
pit, SE SN Sec. 9, T.34 N., R.4 E. (Willman and Frye, 1970).

Willman and Frye (1970) differentiated eight till members
in the Wedron Formation in Illinois. Kempton, DuMontelle, and
(Bass (1971) defined five till units in the Wedron Formation
in the McLean County region. And Johnson, Follmer, Gross, and
Jacobs (1972) recognized four till members in the Wedron
Formation in east-central Illinois. Figure 5 gives the areal

distribution of the named till members as published in

(hddebook Series 9 of the Illinois State Geological

 

Wadswoflh

      
 

 

Jundifferenholed)
‘ \

 

\
\

Snider

 

Frn BotesIOwn

(Unglacuoted)

Glosford Formation .
(undifferennoied)

 

no (Unglacicled)
mourns

 

 

Figure 5 Areal distribution of till formations and

members in Illinois (after Johnson et al.,
1972, and others)

 

ETJE‘} (JO‘I‘LI
five till u
2: been in
On the
312:: lle,
2:: Johnsor
:its for t
:21 Malden
bits 1, 2;
55f- (3) the
iron, 6:
Amp
Either is
liming-t0
Ez‘t of th
sift west
:iSZKil'ga .1
3 3m E
1161:” I
Eye and
the authol
’23”- Unit
is COPPEL
The t

with the ’

11

Survey (Johnson et al., 1972). The reader should note that the
five till units of Kempton, DuMontelle, and Glass (1971) have
not been incorporated into the information on this map.

On the basis of works by Willman and Frye (1970); Kempton,
DuMontelle, and Glass (1971); Johnson, Gross, and Moran (1971);
and JOhnson et a1. (1972) the defined or correlated surface
units for the study area of this thesis are (1) the Tiskilwa
and Malden Till Members of‘Willman and Frye (1970); (2) Till
Units 1, 2, and 4 of Kempton, DuMontelle, and Glass (1971);
and (3) the Glenburn, Snider, and Batestown Till Members of
Johnson, Gross, and Moran (1971).

According tOIWillman and Frye (1970) the Tiskilwa Till
Member is the uppermost till of the western part of the
Bloomington Mbraine (Drift) in the study area. The western
part of the Bloomington Moraine (Drift) is here defined as the
drift west of Bloomington, Illinois. The type section for the
Tiskilwa Till Member is a roadcut in Bureau County known as
the Buda East Section. It is located in the SE SE SW Sec. 31,
T.16 N., R.8 8., 5 miles (8 kilometers) northwest of Tiskilwa
(Frye and.Willman, 1965, page 96, unit 1). In the opinion of
the author the Tiskilwa Till Member can be correlated areally
with Unit 4 of Kempton, DuMontelle, and Glass (1971). Unit 4
is correlated with the Glenburn (Johnson, Gross, and Moran,
1971).

The Glenburn Till Member, which has a possible correlation

with the Tiskilwa Till, is named for the town of Glenburn and

12
its type section is the Emerald Pond Section NE SW SW Sec. 33,

T.20 N., R.12 w., Vermillion County (Johnson, Gross, and Moran,
1971, page 211). Radiocarbon dates indicate that this unit
may be preANoodfordian (JOhnson et al., 1972).
The Malden Till Member is the uppermost till of the
eastern part of the Bloomington Moraine (Drift) and is the
uppermost till of the Eureka and NOrmal Moraines (Drifts) in
the study area (Willman and Frye, 1970). The type section for
the Malden Till Member is in the Malden South Section, SW SE SE
Sec. 5, T.16 N., R.10 E., roadcuts 2 miles (3 kilometers) south
of Malden (Willman and Frye, 1970, pages 185-86). The Malden
Till Member is differentiated into two units (Kempton, DuMontelle,
and Glass, 1971). Unit 2, broadly defined, represents the
uppermost till of the eastern part of the Bloomington Moraine
(Drift), and Unit 1 is the uppermost till of the Eureka and
Normal Moraines (Drifts) (Kempton, DuMontelle, and Glass, 1971).
The Batestown Till Member is correlated with the uppermost
till of the Champaign Moraine (Drift) in the study area
(Johnson et al., 1972). The type section for the Batestown
Till Member is the Emerald Pond Section in Vermillion County,
NE SW SW Sec. 33, T.20 N., R.12 w., (Johnson, Gross, and Moran,
1971, page 211). Unit 3 of Kempton, DuMontelle, and Glass (1971)
was not shown to exist in the study area of this thesis.
However, it has been suggested that the Batestown Till Member
correlates with Unit 3 (Jahnson, Gross, and Moran, 1971; Johnson

et al., 1972). Previously the Batestown Till was called

'1, I.
A U‘
:

'A!%
Not

‘Ififl

Insi-

um

I" I

\n
p‘fi
‘vuv
.

A.

‘H
.5

f5

/ W 7:27 4—"

13
Tazewell by Eveland (1952), and Cerro Gordo and Champaign
by Ekblaw and Willman (1955).

The Snider Till Member was not previously recognized or
correlated with any of the tills in the study area of this
thesis, but the data collected in this study suggests a possible
correlation (see Chapter 4). In the Danville region the Snider
Till is the youngest till and is separated from the Batestown
Till Member below by stratified drift and is named for the
town of Snider, Illinois (Johnson, Gross, and Moran, 1971).

The Emerald Pond Section in NE SW SW Sec. 33, T.20 N., R.12‘W.,
Vermillion County is the type section (Johnson, Gross, and
Meran, 1971, page 211).

Unit 5 of Kempton, DuMontelle, and Glass (1971) is
reported to exist in the study area only as a subsurface till
and was correlated by JOhnson et al. (1972) with the Oakland
Till Member of Ford (in preparation).

Figure 6 summarizes the relationship between Till Members
or Till Units with suggested possible correlations.

 

 

 

 

 

 

 

 

Kempton Johnson JOhnson
Ekblaw Willman DuMontelle Gross et a1.
Eveland Willman Frye Glass Moran (1972)
(1952) (1955) (1970) ,(1971)_, (1971)
‘ 1 Snider ‘Snider
h-Cham ai Malden 2 atestown Cfiatestown
EazeweII Cerro Gordo 3
[ skilwa 4 Glenburn Glenburn
5 *Oakland*

 

 

 

 

 

 

 

Figure 6 Correlated till members
and till units

14

Till Fabric

Holmes (1939) defined till fabric as the space relations
among the component rock and mineral fragments in undisturbed
till and used a quantitative interpretation of these space
relationships in an attempt to eXplain the direction of glacial
ice movement. The technique established by Holmes to determine
fabric has not been modified significantly over the past
thirty years, but refinements in.methods of analysis have been
described during this period of time. Examples include
Harrison (1957a), Kauranne (1960), and Andrews and Shimizu
(1966). Practical uses for till-fabric analysis have expanded
to include determination of the speed of glacial ice movement
(Harris, 1968), stratigraphic variation in tills (Rains, 1969),
reorientation of till by readvancing ice (MacClintock and
lheimanis, 1964), and correlation with landforms such as
drumlins (Wright, 1957) and moraines (HOppe, 1952). Also
variability of till fabrics both horizontally and vertically
has been studied by West and Donner (1957) and Young (1969).

The only till-fabric studies performed near the study
area of this thesis are included in papers by Harrison (1957b),
Smith (1970), and Lineback (1971). The results of the studies
by Smith and Lineback are summarized in Guidebook Series 9
of the Illinois State Geological Survey (JOhnson et al., 1972).
Orientation findings for the Glenburn and Batestown Till
Mbmbers of the Wedron Formation in the Danville, Illinois

region show the Glenburn Till Member to have a southwest

Holmes
son; the c
all and us
slationshi
ice sovemer
fabric has
titty year
scribed c'
Earrison (1
1366). pr
73 include
"iris, 19
Wrientatj
bikinis,
131513th
35599“ 5:

The or
*5 3f thi

31th (197:

14

Till Fabric

Holmes (1939) defined till fabric as the space relations
among the component rock and mineral fragments in undisturbed
till and used a quantitative interpretation of these space
relationships in an attempt to eXplain the direction of glacial
ice movement. The technique established by Holmes to determine
fabric has not been modified significantly over the past
thirty years, but refinements in methods of analysis have been
described during this period of time . Examples include
Harrison (1957a), Kauranne (1960), and Andrews and Shimizu
(1966). Practical uses for till-fabric analysis have expanded
to include determination of the speed of glacial ice movement
(Harris, 1968), stratigraphic variation in tills (Rains, 1969),
reorientation of till by readvancing ice (MacClintock and
Dreimanis, 1964), and correlation with landforms such as
drumlins (Wright, 1957) and moraines (Hoppe, 1952). Also
variability of till fabrics both horizontally and vertically
has been studied by West and Donner (1957) and Young (1969).

The only till-fabric studies performed near the study
area of this thesis are included in papers by Harrison (1957b),
Smith (1970), and Lineback (1971). The results of the studies
by Smith and Lineback are summarized in Guidebook Series 9
of the Illinois State Geological Survey (Johnson et al., 1972).
Orientation findings for the Glenburn and Batestown Till
Members of the Wedron Formation in the Danville, Illinois

reQion show the Glenburn Till Member to have a southwest

gestation
floatation

me ti.
tai'JiQ‘Je O
tile the P
med, me
exuding t
medure C

15;:91‘ 2-

15

orientation and the Batestown to have a south-southwest
orientation (JOhnson et al., 1972).

The till-fabric analysis for this study utilizes the
technique of Holmes (1941). Both dip and strike were measured
while the pebbles were in place in the till. Pebbles were then
removed, measured to the nearest millimeter, and classified
according to shape and lithology. The field and laboratory
procedure of the till-fabric analysis is described in

Chapter 2 .

Till Matrix Composition

The till matrix was analyzed for grain size, clay mineral
composition, and carbonate content by the laboratory of the
Illinois State Geological Survey in Urbana, Illinois. Their
help and coOperation is gratefully acknowledged. The
laboratory procedures used to analyze the till matrix are
described in Chapter 2.

The Illinois State Geological Survey classifies gravel
as particles larger than 2.0 millimeters, sand as particles
between 2.0 and 0.062 millimeters, silt as particles between
0.062 and 0.004 millimeters, and clay as particles smaller
than 0.004 millimeters.

The clay mineral composition is determined by X-ray
diffraction of oriented aggregates for clay-size particles.
Three categories--expandable clays, illite, and chlorite plus
kaolinite--are separated by this tedhnique. The X-ray

diffraction process is also used to determine the carbonate

,whlfl

.‘phv' ‘

a"...

.n-UD

.D- C
.
1| ,1
O" 2
~ i

 

 

4..
no.8}
:37! .
9“.

'Eba.

ht.’

I,
We)

1
2:5,
“4

g

 

16

content. Carbonates are measured in counts per second giving
either calcite or dolomite depending on the angle of analysis.

The till matrix was also described according to color.
Till samples were moistened and a Munsell Soil Color Number
was determined, and a verbal notation of the dry color was

determined.

Data and Analysis Sites

In this study till-fabric and till-matrix composition
analyses were performed on samples collected at 4 to 5 mile
intervals (6 to 8 kilometers) along the trend of the moraines
and at approximately 2 mile (3 kilometers) intervals in the
interlobate area. A discussion on analysis site selection
is presented in Chapter 2.

A total of thirty-eight analysis sites were selected
with thirteen of these in or near the interlobate area. For
each analysis site data collected includes (1) location of the
site; (2) elevation; (3) type of exposure (roadcut, pipeline
trench, etc.); (4) depth of sample; (5) topography of the
area including location of site with regard to the outline of
the moraine (proximal, distal, or central); (6) till-pebble
data which includes the size, shape, long-axis orientation, and
lithology of each pebble; and (7) till-matrix composition data
which includes the till color, grain-size distribution, clay
mineral composition, and carbonate content. The data for all

thirty-eight analysis sites are included in the Appendix of
this thesis.

17

The relationship between landforms and sedimentary
parameters can be found extensively in the literature of glacial
geomorphology. For example, Hoppe (1952) carefully described
the location of each of his till fabrics in terms of its
location with respect to the outline of the moraine or hummock
from which it was taken. Such descriptions made it possible
for him to state certain relationships between sediments and
landforms. Rains (1969) used the sedimentary parameters of
till-fabric analysis to confirm the existence of two till
units stratigraphically at a particular location. Anderson
(1955) used the sedimentary parameter of pebble lithology and
reports that pebble lithology is determined largely by the
position and distance of the source area relative to the
direction of ice movement and can be used to distinguish tills
from different ice lobes. Willman and Frye (1970) used
sedimentary parameters to differentiate the rock-stratigraphic
units defined in Illinois.

The purpose of this thesis is to analyze and describe
the relationships that exist between certain sedimentary
terameters and landforms. The landform unit in this thesis
is the morphostratigraphic unit (end moraine). The sedimentary
[arameters are pebble orientation, pebble lithology, and
till-matrix composition. This thesis will analyze and describe
the relationships between four morphostratigraphic units in
central Illinois and certain sedimentary parameter data

gathered from thirty-eight analysis sites along these units.

18

Justification for the Study

 

Till-fabric analysis and till-matrix composition
analysis have proved to be important and meaningful field and
laboratory techniques in glacial geomorphology. In addition
to adding to knowledge of the glacial geomorphology of an
area, they may reveal eSpecially significant relationships
between landforms and sediments. The writer knows of no
till-fabric studies that apply the concept to interlobate areas.
Sudh application may make it possible to determine at least
in part ice behavior in interlobate areas and to better
understand the nature of deglaciation in such regions.
Finally, the area selected in Illinois is especially favorable
for this analysis because the tOpography has been carefully
mapped and the landforms are a part of one of the best under-

stood Midwestern glacial landscapes.

n ,
"’f'
«uh.

17“".

'“1

Eve

if»
k,‘:

Chapter 2
FIELD WORK AND LABORATORY ANALYSIS

Selection of the Study Area
Introduction
The primary objective of this study is to determine
relationships between morphostratigraphy and certain aspects
of rock stratigraphy including pebble orientation, pebble
lithology, and till-matrix composition. Such relationships
would probably be most revealing (l) where the end moraines
have good topographic expression both vertically and
laterally, (2) where the proximal and distal boundaries of
end moraines are reasonably well defined, (3) where the end
moraines were formed by two distinct lobes of glacial ice,
and (4) where the end moraines of two lobes merge into an
interlobate area. An area that satisfies all these criteria
is located in central Illinois, where the Eureka, Normal, and
Bloomington Moraines (Drifts) merge with the Champaign

Moraine (Drift) in what appears to be an interlobate area.

Study Area
Willman and Frye (1970) defined and delineated the
Bloomington, Champaign, Eureka, and Normal Moraines (Drifts)
(see Figure 4, in pocket). The study area for this thesis
is shown on Figure 7 and can be delineated as follows: The
Bloomington Moraine (Drift) was studied from the McLean

County line on the west to the interlobate area in eastern

l9

20

 

 

I'_———

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

I McLEAN
Ell
as
h 1
ET
. BPS
BOB
' 89.0
,:§, 307
305
EXPLANATION C
'E EUREKA MORAINE '
NORMAL MORAINE
BLOOMINGTON MORAINE ° 5 '° ””3
(2 g IOKM

m CHAMPAIGN MORAINE A
.83 ANALYSIS SITE

 

Figure 7 Morphostratigraphic units of the study area
with general location of analysis sites

 

21
MCLean County. The Champaign Moraine (Drift) was studied in
the area between its two points of dissection by the Sangamon
River approximately marked by analysis site locations C6 and
C1. The Eureka Moraine (Drift) was studied from the area of
its dissection by the Mackinaw River near analysis site EB2
to the interlObate area in eastern McLean County. And the

Normal Mbraine (Drift) was studied throughout its entire extent.

Selection of Analysis Sites
Introduction

The Map "Woodfordian Moraines of.Illinois" (Figure 4,
in pocket) summarizes more than seventy years of refinement
in the mapping of the surficial landforms of the study area
of this thesis. Leverett (1897, 1899) first mapped the
Pleistocene landforms of this area, and the Bloomington Morainic
System.and Champaign Morainic System*were named by him.
Leighton and Ekblaw (1932) and Ekblaw (1941, 1959) revised
and updated the mapping of Pleistocene deposits in the study
area, adding the Normal Moraine. Further revisions by
u; M. Leighton and J. A. Brophy (1961) altered the extent
of the Normal Moraine. ‘Willman and Frye (1970) defined the
Eureka Mbraine and established the extent of the Bloomington,

Champaign, and Normal Moraines to their present positions.

Analysis Sites
Analysis sites were spaced 4 to 5 miles (6 to 8 kilometers)
apart along the trend of the Bloomington and Champaign

Moraines (Drifts), but because of the close and problematical

22

relationship between the Eureka and Normal Moraines (Drifts)
the 4 to 5 mile (6 to 8 kilometers) interval was alternated.
The series of alternating sites appears justified in this area
because according to Willman and Frye (1970) the Eureka and
Normal Moraines (Drifts) are both part of the same rock-
stratigraphic unit, the Malden Till Member. In the inter-
lobate area where greater definition and refinement of
relationships is sought, the interval between analysis sites
was reduced to a l to 2 mile (1 to 3 kilometers) interval.
A total of thirty-eight general analysis locations was
selected along the moraines (see Figure 7).

Once a desirable general location for an analysis site
was selected, two factors were considered before the
specific location was determined. First only an exposure
(such as a railroad cut, roadcut, pipeline trench, or borrow
pit) within the moraine deep enough to reveal till below
the zone of calcium carbonate (CaCO3) leaching was considered
to be a suitable location for analysis (see Figure 8). The
surface till of the study area lies stratigraphically below
the Richland Loess (Willman and Frye, 1970). The thickness
of loess on top of the moraines of the study area ranged from
less than 1 foot (0.3 meters) to approximately 8 feet (2.3 meters)
in depth. Three feet (1 meter) of loess was very canmon.
The surface of the calcareous zone was usually found to be
about 4 feet (1.3 meters) and never exceeded 5 feet (1.5 meters)

below the top of the cut or excavation.

23

Figure 8 Examples of analysis sites

Figure 8A Pipeline trench
. Six foot deep trench in Malden Till

at analysis site E7; (See Figure 7
for location)

Figure 8B Borrow pit
Borrow pit exposure of Shamrock

Till along I-74 at analysis
site B4; (See Figure 7 for
location)

24

 

 

25

Figure 8 Examples of analysis sites

Figure 8C Roadcut with dig
Twelve foot roadcut exposure
showing Richland Loess overlying
Malden Till at analysis site N2

Figure 8D Close up of dig illustrating dip measurement
Brunton compass measuring dip of pebble
embedded in Snider Till at analysis site
BD7

26

 

 

Figure 8C

 

 

 

Figure 8D

The
below 1::
25 fee:
selectic
mount
hat, ii
to have
'2; grav:
was sele
figs in
UP meche
in most
Part of
such a j
have mo:
Maria;
“Sting

me :11;

27

The average depth of till analysis was 8 feet (2.3 meters)
below the original surface but this figure ranged from 4 to
25 feet (1.3 to 7.5 meters). A second factor considered in the
selection of an analysis site was its location relative to the
surrounding topography. Glen, Donner, andfiWest (1957) suggest
that, if care is taken to select deposits that do not appear
to have been seriously disturbed since deposition, reorientation
by gravitational movement can be minimized. When an exposure
was selected as suitable, an attempt was made to locate the
dig3 in such a way that reorientation of the fabric by slides
or medhanical movement was minimized. This was accomplished
in most cases by selecting satisfactory exposures in the higher
part of the moraine in the area of the analysis. By selecting
such a location, the till under analysis could be assumed to
have most likely remained unmoved or unaffected in any way by
material that had moved as a result of gravitational mass
wasting since its time of deposition. Thus, the fabric of

the till would represent its original depositional environment.

Field Technique
Introduction
Most of the field data for this thesis was collected

during the summer of 1971. The field procedure was initiated

 

3

A "dig" is here defined to be the excavation into the
side of an exposure necessary to create a suitable working
surface for a till-fabric analysis (see Figures 8C and 8D).

if the
1hits

[See F

H‘

28

by the selection of an analysis site. Each location was
identified by a field note number which was to identify the
analysis site. The letter B was used to identify analysis
sites along the trend of the Bloomington Moraine (Drift),
C was used for Champaign Moraine (Drift), E for Eureka
Moraine (Drift), and N for Normal Moraine (Drift). The
letters EB refer to an analysis site located areally on the
Eureka Morphostratigraphic Unit but in a lower rock-stratigraphic
unit than the top till of the Eureka Moraine (Drift). In the
interlobate area, which was defined by Willman and Frye (1970)
as Bloomington Moraine (Drift), the letters BP and BB were
used to identify analysis sites. BP denotes defined Bloomington
Moraine (Drift) on the Peoria Sublobe side of the interlobate,
and BD denotes Decatur Sublobe side of the same unit. The
boundary between Peoria Sublobe side and Decatur Sublobe side
of the interlobate is defined as a line connecting the upper
limits of two intermittent streams as they bisect the interlobate
(see Figure 9). Along with each letter designation is a
number which identifies a specific location on the morphostrati-
graphic unit.

The identifying number, legal land description, elevation,
type of exposure, depth of sample below the top of the
exposure or cut, and tapography were recorded for each analysis
site (see the Appendix). TOpography was described by slope
develOpment in the area of the analysis site and location with

respect to the outline of the moraine. Slope develOpment was

29

 

 

LEGEND

— —"" COUNTY LINE

”“' ‘"“' "" INTERMIT TENT
STREAM

norm

0 8P8 ANALYSIS SITE

'57! 'BP8

 

o’ o /"I
0 U /.-'
BPII ’ 2 //"
< E's? - BD8
NI W 8ro // I
,y\ /
. BP7 / . BD7

)

./
o ._,/' |
86 o 805
j l
0
C6

INTERLOBATE MAP
gzaaézéinz “Les

0 | 2 KM.
:35

“CS

 

Figure 9 Interlobate map

 

‘l
y:

Ila:

('3
Q

30
given by letter designation according to the scheme of the

U.S.D.A. Soil Soncervation Service Soil Surveys (see Figure 10).

 

Figure 10 Slape develOpment classification

Location of the analysis site with respect to the outline

of the moraine was described as proximal, distal, or central.

Till-Fabric Analysis

At each site selected a horizontal surface approximately
3 feet square (2500 square centimeters) was excavated
(see Figure 8D). The surface was cleared and leveled with a
mattock and brushed with a small broom to expose the top
surface of any pebbles at that level. The matrix of till
around each pebble was then carefully removed with a pocket
knife in an effort to determine the long axis of the pebble.
Approximately 4 pounds (1.8 kilograms) of the excavated till
matrix was collected and bagged for later laboratory analysis
as the pebbles were uncovered. While the pebble remained in
Place within the till matrix, the direction of the long axis
was marked with a pencil line on the pebble. The Brunton

compass was used to determine the direction of the pebble's

mg axis
to the m
i dip 01
he seas:
field wa:
lessee 0:
30th mea:
Appendix
envelope
:ebbles I
asecond
ntll a :
(see Fig
afifty.]
Orientat:

011 c
the pebb:
is actua:
second 1‘

Each
The 151301:

vertical :

31

long axis to the nearest 5 degrees in the l80-degree sector
to the north of east-west. The clincmeter measured the amount
of dip of each pebble to the nearest 5 degrees (see Figure 8D).
The measurement of pebbles to the nearest 5 degrees in the
field was utilized because it appears to provide an acceptable
degree of accuracy for till-fabric studies (Harris, 1969).
Both measurements were recorded in the field notes (see the
Appendix). The pebble was then removed, placed in an
envelope, and filed for later laboratory analysis. After all
pebbles of one layer had been measured, recorded, and filed,
a second lower level was scraped clean and the process repeated
tmtil a random.sample of fifty pebbles had been collected
(see Figure 11). Harris (1969) illustrates statistically that
a fifty-pebble sample is usually sufficient to show preferred
orientation.

On occasions when the long axis of a pebble was vertical,
the pebble's long axis orientation measurement (strike)
is actually a measurement of the orientation of the pebble‘s
second longest axis.4 Pebble orientation data is presented in

the Appendix and summarized graphically on Figure 14 (in pocket).

Laboratory Analysis of Pebbles
Introduction
Each pebble collected was analyzed in the laboratory.

The laboratory procedure included (1) measuring the three

 

4An example of a study that discusses pebbles with a
‘Vertical long axis orientation is Hoppe (1952).

32

Figure 11 Random sample of fifty pebbles
The fifty-pebble sample from analysis
site N1 serves as an example to
illustrate size and shape of pebbles
for an analysis site location of
“this study .

Figure 12 Representative pebble shape categories
1 and 2 -- Tabular
3 and 4 - Rhombohedroid
5, 6, and 7 -- Wedge-form
8 and 9 -- Ovoid

 

33

 

 

 

 

1.

z ‘. .1 4. r s ,

0 fl . o . o .
,I n. I! I4 r“ a
D 4 D 0 a o a o A .
U 2‘- 1\ 2 -V ‘ r 1‘!

o a O . . O I O
3! 3?. 33 3‘ 3' 2v J7 5! l,
0 O 0 o g o a a a t

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9 Q Q s I O 0 C I o

 

 

 

 

 

 

 

 

 

 

 

 

‘_
Figure 12

Inese lab

sumarize

For
categorie
ms and
Of his pe
Weld, ta
I519mm
Slightly
Eelmes' (
(1923, 1:
Hermon}
to descri
Lake 1‘ng

metre:

34
dimensions of each pebble to the nearest millimeter,
(2) classifying the pebble according to shape (see Figure 12),
and (3) identifying and classifying each pebble's lithology.
These laboratory data are presented in the Appendix and

summariZed in Tables 2, 5, and 7.

Pebble Shape

For this study pebble shape was divided into nine
categories (see Figure 12). Holmes (1941) used six major
forms and four categories of roundness to describe the shape
of his pebbles. The six major forms were called discoid,
ovoid, tabular, wedge-form, rhombOhedroid, and varihedroid.
The roundness classifications were called sharply angular,
slightly rounded, moderately rounded, and well rounded.
Holmes' (1941) categories were based on the work of wentworth
(1923, 1936), Wadell (1932, 1936), and Tester (1931).
Wentworth (1936) used thirteen descriptive categories of shape
to describe glacial pebbles from the Baraboo and Devil's
Lake region of Wisconsin. Holmes (1941, plate 1, page 1355)
illustrates seventeen of his twenty-four possible categories
of form and roundness. Holmes (1941, page 1307) states:
"tabular and discoid stones should be grouped together." For
this reason and because it is very difficult to differentiate
the sharply angular to slightly rounded varihedroid from the
sharply angular to slightly rounded wedge-form, the discoid
and varihedroid forms of Holmes (1941) were not used in this

study. Four forms--tabular, rhombohedroid, wedge-form, and

hoe wed
six, and
five or s
sane snap
l'ne nurloe
:ouniness
and the n

1“: round

Elmlated
handed .‘

.v

$9813.

Class
59955 It:
Hiltheps (
in Way

53161911 va

35

ovoid--were expanded into nine shape categories (see Figure 12).
The first and second are tabular shapes, number one arrowhead
in form, number two less pointed, but both flat. Rhombohedroid
shapes were classified in two groups and numbered three and
four. The number four was more elongated than number three.
Three wedge-form shapes were recognized and numbered five,

six, and seven, with the number six shape more elongated than
five or seven. Numbers five and seven have basically the

same shape but were differentiated on the basis of roundness.
The number five shape would include all pebbles with a
roundness classified as moderately rounded or well rounded,

and the number seven shape would be more angular and include
the roundness categories classified as slightly rounded or
sharply angular (Holmes, 1941). The ovoid forms were

assigned the numbers eight and nine and differ only in the
ratio of the two longest dimensions, the latter being more
elongated. The data on pebble size and pebble shape are
included in the Appendix but will not be analyzed in this

thesis.

Pebble Lithology
Classification of the lithology of glacial pebbles has
been a research tool in glacial geomorphology for many years.
Milthers (1942) studied the lithology of glacial pebbles
in Norway and the Baltic region of Denmark; Holmes (1952)

studied variations in glacial pebble lithology in New York;

36
and Anderson (1955) published an important work on the pebble
lithology of the Marseilles till sheet in northeastern
Illinois. More recently Ancin and Jacobs (in Johnson et al.,
1972) classified the lithology of glacial pebbles from tills
in east-central Illinois.

In this study only the elongate pebbles measured for
orientation were classified lithologically. Thus, the
sample was not a random sample. Since each sample of fifty
pebbles in this study was biased by the same collection
technique, they can effectively be compared lithologically.
However, future investigators using the sedimentary parameter
of pebble lithology should be aware of the restrictions
placed on the pebble samples of this study which were
classified lithologically.

Classification of each pebble's lithology was accomplished
by fracturing each pebble to expose a fresh surface. The
exposed fresh surface was then examined by hand lens and if
necessary through a binocular microscoPe. Each pebble was
identified and classified (see the Appendix). Five lithologic
categories were recognized: crystalline, carbonate,
noncarbonate elastic, chert-flint, and other. The crystalline
pebbles were dominantly granites, basalts, and quartzites,
but the category includes all igneous and metamorphic
crystalline pebbles. Carbonate pebbles include limestone,
dolomite, and all gradations between these such as limey

dolomite, dolomitic limestone, and cherty dolomite. The

37

noncarbonate elastic pebbles were dominated by shales and
siltstones but included sandstones and all gradations between
these three categories. The chert-flint group of pebbles
includes only those lithologies. The lithologic classification
of the remaining pebbles was diverse and statistically
insignificant. These were placed together in the category

termed other.

Laboratory Analysis of Till Matrix
Introduction

Laboratory analysis of the till-matrix samples collected
at each analysis site was performed to characterize certain
physical and compositional properties of the sediment. The
laboratory analysis provided numerical data on grain size,
percentage of sand, silt, and clay; clay mineral composition,
percentage of expandable clay minerals, illite, and chlorite
plus kaolinite; and carbonate content, counts per second of
calcite and dolomite. Clay mineral composition and carbonate
content was determined by X-ray diffraction analysis. The
color of a moist sample of the till matrix for each analysis
site was identified using the Munsell Soil Color Charts (1971),
and in addition a descriptive color was recorded for a dry
sample. The data from the laboratory analysis for each
.analysis site are given in the Appendix and summarized in
Tables 1, 4, and 6.

Gross (1969, pages 33-37) has described the grain-size

analysis and X-ray diffraction analysis techniques used by

he Illinoi
(oral comm:
ox'ified w
sections 0:
I-ray Diff

ark of D.

The g
was deter:
State Geo:
iMlysis.
geolOgiQa:
fem othe:

Samp
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The
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to a 1001
13003111;

In

‘P

‘or Us.

4" CleEre.

38

the Illinois State Geological Survey and has given permission
(oral communication, June 1972) for use of a slightly
modified version of his description in this thesis. The
sections of this chapter, entitled Grain-Size Analysis and
x-ray Diffraction Analysis which follow are largely the

mwome.mmm

Grain-Size Analysis

The grain-size distribution of the till-matrix samples
was determined in the sedimentation laboratory of the Illinois
State Geological Survey by a combined hydrometer and sieve
analysis. This technique has been standardized by the
Geological Survey so that the data may be compared with data
from other parts of the state of Illinois.

Samples from each analysis site were first air-dried in
the laboratory. The original sample was split into three
subsamples, one for grain-size analysis, one for X-ray
analysis, and one to be stored. Fifty-five grams of sample
were used for grain-size analysis.

The sample was transferred to a milkshake mixer,

25 milliliters of 4 per cent sodium hexametaphosphate (Calgon)
were added, and the mixer was filled with distilled water.
.After thirty minutes of mixing, the sample was transferred

'to a 1000 milliliter settling cylinder. After filling to
21000 milliliters with distilled water, the cylinder was
‘Jigorously Shaken and placed in a water bath heated to

30 degrees Centigrade. After three hours, if no flocculation

:as observe
single hyd:
fifty-eighl
calibrated
directly 1

The s
sieve to r
arotap ma
2.00-nilli

The c
5'light of
W give ti
2.00-nilli
the sand (
“light of
Dementags
silt (0.01
the 511m 0:
The sand,

in mEasu

The
indieitio
if: dete

Clay frag

39

was observed, the sample was reshaken for five minutes. A
single hydrometer reading was taken after one hour and
fifty-eight minutes. The hydrometers have been specially
calibrated for this temperature so that they can be read
directly in grams of clay present in the sample.

The sample was then wet-sieved through a S3-micron
sieve to remove the sand. The sand was dried and sieved on
a rotap machine for fifteen minutes to remove the greater-than-
2.00-millimeters and the greater-than-GZ-micron fractions.

The original SS-gram sample weight was divided by the
weight of the greater-than-2.00-millimeters-size fraction
to give the percentage of gravel. The weight of the less-than-
2.00-millimeters-size fraction was divided by the weight of
the sand (2.00 millimeters to 0.062 millimeters) and the
weight of the clay (less than .004 millimeters) to give the
percentages of sand and clay respectively. The percentage of
silt (0.062 to .004 millimeters) was obtained by subtracting
the sum of the sand and clay percentages from 100 per cent.
The sand, silt, and clay percentages total 100 per cent and

are measurements of the less-than-Z.00-millimeters fraction.

X-ray Diffraction Analysis
The composition of the clay mineral fraction and an
indication of the relative abundance of calcite and dolomite
were determined on oriented aggregates of the less-than-Z-micron

clay fraction by x-ray diffraction procedures. These analyses

40

were performed by Dr. H. D. Glass in the clay mineralogy
laboratory of the stratigraphy section of the Illinois State
Geological Survey.

Approximately 35 grams of the whole sample were placed
in a loo-milliliter beaker and distilled water added. The
beaker was vigorously stirred, and a small portion of the
suspension was immediately decanted into another beaker.

This procedure was repeated several times and the sand and
gravel fractions discarded. The clay fraction was then
dispersed. If flocculation occurred, the water was carefully
decanted off, more distilled water added, and the beaker
restirred. This was usually sufficient to disperse the sample,
but occasionally a little sodium hexametaphosphate was added.

After settling for twenty minutes, a portion of the
less-than-Z-micron suspension.was removed with a pipette, placed
on a glass slide, and air-dried.

The oriented aggregate slides were analyzed with a
General Electric XRDbS diffraction unit coupled with a
horizontal goniometer and a recording diffractometer. The
slides were run after exposure to ethylene glycol vapor.
Quantitative analysis of the percentages of eXpandable clay
minerals, illite, and chlorite plus kaolinite, and relative
abundance of calcite and dolomite has been standardized by
the Geological Survey so that these data may be compared with

data from other parts of the State of Illinois.

41

The eXpandable clay minerals are identified by the
presence of a peak at approximately 17 Angstroms after treatment
with ethylene glycol. These minerals include montmorillonite
but are here principally formed by eXpandable vermiculite and

#w‘hwh.,w -r-‘Md --"-

chlorite as well as their mixed lattice intermediates.

Illite is identified by the presence of a 10 Angstrom
peak, and is defined as a nonexpanding and noncollapsing
lO Angstrom clay mineral.

Chlorite plus kaolinite is calculated by the intensity
of the 7.2 Angstrom reflection. Chlorite is the dominant
mineral and is Characterized by a 14 Angstrom periodicity.
A trace of kaolinite was present in.some samples. The first-order
kaolinite reflection and the second-order chlorite reflection
both occur at about 7 Angstroms, but the second-order kaolinite
peak and the fourth-order chlorite peak could be observed
separately and the presence of kaolinite thus noted.

To calculate the clay mineral percentages, a base line
was drawn on the log-normal-diffraction Chart. The differences
in intensity, measured in counts per second, between this base
line and the 7, 10, and 17 Angstrom peaks were then recorded.
The counts noted for illite were multiplied by three, the
counts noted for chlorite plus kaolinite were multiplied by
two, and the counts for the eXpandable clay minerals were
left unchanged in order to equalize the scattering difference
between the different clay minerals. These ratios were then

converted to 100 per cent.

iiridir
second;
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index I
in the
first
to 14
clay n
his 1
the 7
fine In;
sectic

10: be

neasun
Count.
neasu

the p

42

A diffraction intensity (DI) ratio was calculated by
dividing the intensity of the illite peak, in counts per
second, by the intensity of the chlorite plus kaolinite peak,
in counts per second. This DI ratio is used as a numerical
index of weathering. Illite is not appreciably weathered
in.the‘Woodfordian Substage of Illinois, but one of the very
first effects of weathering is the alteration of chlorite
to 14 Angstrom vermiculite and eventually to an eXpandable
clay mineral at about 17 Angstroms (swelling chlorite).

This loss of Chlorite is reflected by a loss in intensity of

the 7 Angstrom peak and causes the DI ratio to increase.

The Diffraction Intensity ratio is most useful in a vertical
section to compare samples within a profile. However, it should
not be used as an "index fossil."

The relative abundance of calcite and dolomite was
measured from the oriented slide. Calcite is measured in
counts per second at 29.4 degrees 2-theta and dolomite is
measured at 30.9 degrees 2—theta. These measurements reflect
the percentage of the minerals present and also the particle
size, crystallinity, and orientation of the minerals. Thus,
the measurements are not true percentages. Preliminary
results of work by Moran and Gross (oral communication,

July 1972) indicate that calcite counts per second as
determined by these x-ray methods correlate very well with true
calcite percentages as determined with the Chittack apparatus

(Driemanis, 1962). The correlation coefficient, based on

43

134 sets of duplicate analyses, for these two parameters is
.90, which indicates a very high degree of correlation. The
calcite counts per second should be divided by 3.6 (the slope
of the regression line for the correlation) to get a true
percentage of calcite. The correlation of dolomite counts
per second to true per cent dolomite is not as good, with

a .56 correlation coefficient. This relationship is almost
one to one; the slope of the regression line is .97, which
means that dolomite counts per second are approximately

equal to true per cent dolomite.

This rapid clay mineral and carbonate X-ray procedure
is particularly well suited for working with large numbers
of samples. It is true that the numbers reported may not
represent actual clay mineral percentages, but these are
reproducible data which can be used for stratigraphic
correlations.

Quantitative estimation of the amount of each clay
mineral component present is difficult and an approximation
at best. The procedure described above is based on the
assumption that the greater the quantity of a particular
mineral, the more intense the diffraction peaks of that
mineral will be. However, other factors such as particle
size, crystallinity, and the degree of orientation on the
slide also influence the peak intensities and thus limit
the preciseness of quantitative estimates. Therefore, it

must be realized that the clay mineral data presented in this

44
study are useful for stratigraphic correlation, but not

necessarily as precise measurements of clay mineral content.

Color Analysis

The color of the till-matrix samples was determined by
comparing a moist sample of the till matrix with the chips
of Munsell Soil Color Charts. The Munsell Soil Color Book (1971)
has seven charts containing 196 chips. The color of each chip
has a three-variable description. The three variables are
hue, value, and Chroma. The hue notation of a color indicates
its relation to red, yellow, green, blue, or purple; the
value notation indicates its lightness; and the chroma
notation indicates its strength or departure from a neutral
of the same lightness (Munsell Color Company, 1971). An
example of a Munsell color notation.would be 7.5YR 5/6,
with the 7.5YR.representing the hue as a combination of
yellow and red, 5 as the value, and 6 as the chroma.

The technique previously described in this study for
X-ray diffraction analysis required the use of a slide that
contains a dry sample of the clay fraction of the till-matrix
sample. This slide was used to indicate a dry sample color
because the slides can be compared for color easily. The
descriptive words used included the following: yellow tan,
gray brown, violet, peach, salmon, green gray, gray, olive,

gray tan, tan, buff tan, and red brown.

Chapter 3

CHARACTERISTICS OF THE
EUREKA-NORMAL MORPHOSTRATIGRAPHIC UNIT

Introduction

 

The individual morphostratigraphic units considered in
Chapters 3, 4, and S of this thesis were delineated on the
basis of definitions by Willman and Frye (1970). Portions
of the Eureka, Champaign, and Bloomington Moraines (Drifts)
and all of the Normal Moraine (Drift) were studied (see
Figure 7). This chapter is concerned with the characteristics
of the Eureka and Normal Moraines (Drifts).

By definition a morphostratigraphic unit is identified
by the surface form it displays (Frye and Willman, 1960,

1962). A topographic boundary which delineates and separates
the Eureka and Normal Moraines (Drifts) as two separate
morphostratigraphic units is not apparent through field
observation or map study except possibly in the area around
Arrowsmith, Illinois. Therefore, these two morphostratigraphic
units will be considered as one unit called the Eureka-Normal
Moraine (Drift). Figure 13 (in pocket) is a Peoria

l:250,000 topographic contour map that may be referred to

when altitudes associated with the study area are described.
The distal base of the Eureka-Normal Moraine (Drift) in the
study area is approximately marked by the 800 foot (243 meters)

contour west of the city of Normal and by the 825 foot

45

46
(247 meters) contour east of the city. The proximal base of
the Eureka-Normal Moraine (Drift) closely parallels the
800 foot (243 meters) contour except in the area where the
FletChers Moraine (Drift) exists (see Figure 4, in pocket).
Here the proximal base of the moraine ranges from 800 feet
(243 meters) to over 920 feet (276 meters) where the Eureka
and Fletchers Moraines (Drifts) are adjoining.

The maximum relief in the study area is found in
sections 7 and 18, T.23 N., R.6 E., where the crest of the
Eureka-NOrmal Moraine (Drift) is 150 feet (45 meters) higher
than the distal margin. At an altitude of approximately
950 feet (285 meters) this crest is the highest elevation
in the study area. The rolling distal slopes are steeper
than the more gradual gently leping proximal slopes and the
tops of the moraines are undulating. Within the moraine the
more rugged topography is generally located in regions where
streams have dissected or eroded the moraine. Thus, the present
topography is the result of both glacial deposition and
stream dissection. Possibly the best example of an area
within the Eureka-Normal Moraine (Drift) that shows such
effects is the Mackinaw River'Valley (see Figure 13, in pocket).
The Appendix contains a statement on the tOpography at
each analysis site.

The trend of each moraine was determined to be a line
connecting the crests of each morphostratigraphic unit as
illustrated on Figure 14 (in pocket) and called the peak of

the moraine. Fifteen analysis sites were selected along the

47
trend of the Eureka-Normal Moraine (Drift) (see Figure 7).
Six (El, E3, E5, E6, E9, and EB2) were located in a central

position on the moraine; two (E7 and Ell) were located on the
proximal slope; and seven (E4, E8, E10, N1, N2, N3, and N4)
were located on the distal 310pe. The average altitude of the
crests of the exposures used for analysis is 830 feet

(248 meters). The average depth of analysis below these crests
was 6 feet (2 meters). One analysis site (EB2) was strati-
graphically below the top till of the Eureka Moraine (Drift).
The stratigraphic relationships between the till at E82 and
the till at E10 will be discussed where the Congerville Section
is described later in this chapter. Data from these fifteen
analysis sites will be presented and analyzed in this chapter
and later compared with comparable data from the other
morphostratigraphic units under consideration so that the

basic problem of relationShips can be examined.

Physical Characteristics of the Till Matrix

 

The Eureka-Normal Moraine (Drift) represents some of the
deposits of the Peoria Sublobe of the Lake Michigan Lobe
(see Figure 3) deposited during the Woodfordian Substage of
the Wisconsinan Stage in central Illinois (Willman and Frye,
1970). The Eureka-Normal Moraine (Drift) is a part of the
Malden Till Member of the Wedron Formation (Willman and
Frye, 1970) (see Figure 5). Willman and Frye (1970) describe
the physical characteristics of the Malden Till Member as a
silty, locally sandy, yellow gray to gray tan till bounded
above by the Yorkville Till and below by the Tiskilwa Till.

48
This till can be correlated areally in McLean County with

Unit 1 of Kempton, DuMontelle, and Glass (1971). These authors
summarized the physical characteristics of Unit 1 as a tan

or yellowish brown oxidized till or a gray or olive gray
unoxidized till with average grain-size distribution of

15 per cent sand, 49 per cent silt, and 36 per cent clay,

with average clay mineral composition of 2 per cent
montmorillonites, 82 per cent illite and 16 per cent chlorite
and kaolinite, and with a carbonate content of 10 counts per
second calcite and 16 counts per second dolomite. The percent-
ages given in the above description are based on thirty samples
from McLean County. Willman and Frye (1970, Table 3,

pp. 169-170) reported the results of similar analyses for four
samples, two from the Eureka Moraine (Drift) and two from the
Normal Moraine (Drift). Averages of the results of these four
analyses show a grain-size distribution of 15 per cent sand,

41 per cent silt and 44 per cent clay, a clay mineral
composition of 6 per cent eXpandable clays, 81 per cent illite,
and 13 per cent kaolinite and chlorite, and carbonate content
of 7 counts per second calcite and 23 counts per second
dolomite. Location of the type section for the Malden Till

Member can be found in Chapter 1 (see page 12).

 

SMontmorillonite has been used by some I.S.G.S. authors
in place of expandable clays. Data produced by x-ray diffraction
analysis at the Illinois State Geological Survey on clay
minerals is comparable for both categories. (H. D. Glass oral
communication).

49

The physical characteristics of the Malden and Unit One
Tills are described in terms of the same variables investigated
in this study. Table 1 summarizes the data, on the physical
characteristics of the till matrix for the Eureka-Normal
Moraine (Drift), found in the Appendix. Data on color,
grain size, clay mineral composition, and carbonate content for
the fifteen analysis sites arranged from east to west along
the trend of the Eureka-Nbrmal Moraine (Drift) are included
in this table (see Figure 7). Analysis site E82 is
included here because its location is in the area of the Eureka
Moraine (Drift), but the till lies stratigraphically below the
t0p till unit. The till overlying EB2 is described by the
data for analysis site 810. A discussion of the stratigraphic
relationship between these two till members is presented later
in this chapter where the Congerville Section is described.

All till samples collected along the Eureka-Normal Moraine
(Drift) were calcareous and oxidized. The average depth of
leaching on well-drained level upland sites is about
4 feet (1.3 meters). The oxidation is reflected in the tan to
buff tan color (2.5Y 5/4) that may grade into unoxidized till
at a depth ranging from 12 to 15 feet (3.6 to 4.5 meters).
Average depth of analysis for Eureka-Normal till samples was
approximately 6 feet (2 meters) and ranged from 5 to 10 feet
(1.5 to 3 meters) below the crest of the exposure.

The averages reported in Table l for all Eureka-Normal
analysis sites, exclusive of E82, are remarkably consistent

with the averages for Eureka and NOrmal Moraine (Drift)

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51

samples for the Malden Till Member of Willman and Frye (1970)
and with the averages for Unit 1 of Kempton, DuMontelle, and
Glass (1971). The only notable difference exists in the sand
content of the grain-size distribution which shows sand content
somewhat higher than the 15 per cent reported by both Willman
and Frye (1970) and Kempton, DuMontelle, and Glass (1971).
Howevers Willman and Frye (1970) described the Malden Till as

a "silty locally sandy till" and the locally sandy condition
appears to exist at analysis sites El, ES, E6, E7, and EB (see
Figure 7). The till-matrix composition at analysis site N3

is somewhat anomalous, but the color difference and high cal-
cite content are within the ranges for the Malden Till Member
reported for these variables by Willman and Frye (1970). The
averages of the numerical data in Table l for the Eureka-Normal
till samples are also comparable to the numerical data presented
for the Snider Till Member in the Danville, Illinois region
(JChnson, Gross, and Moran, 1971; Johnson et al., 1972,

Table 2, page 7). The relationship between Malden and Snider
Till will be discussed in Chapters 4 and S of this thesis.

Thus, the rock-stratigraphic unit to which the Eureka-Normal
Moraine (Drift) in the study area of this thesis is assigned is
the Malden Till Member of the Wedron Formation. This conclusion,
whiCh is consistent with the findings of Willman and Frye (1970),
is based on the high degree of correlation between the physical
characteristics of the till matrix reported in Table 1 and

the description of the Malden Till.

52
Characteristics of Till Pebbles
Introduction

Data on pebble lithology, long-axis pebble orientation,
size, and shape were collected for a fifty-pebble sample at
each of the fifteen analysis sites along the trend of the
Eureka-Normal Moraine (Drift) (see the Appendix and Figure 7).
This study is concerned with the relationship between long-axis
pebble orientation, pebble lithology, rock stratigraphy, and
morphostratigraphy. Pebble size and shape data are included.
in the Appendix but will not be analyzed in this thesis.

Holmes (1941) was the first in this country to correlate
long-axis pebble orientation with the direction of ice move-
ment associated with an area of ground moraine in New York.

He recognized both parallel and transverse patterns of long-
axis pebble orientation and associated these with the direction
of ice movement. Hoppe (1952) correlated the parallel and
transverse patterns of long-axis orientation to ridge trends of
hummocky moraines in Sweden but found little or no pebble
orientation in the hollows between ridges. Wright (1962)
correlated patterns of pebble alignment with the axes of
drumlins in Minnesota and found them to parallel one another.
Today most if not all investigators using the teChniques of
till-fabric analysis would agree that there is a strong
tendency for the long axis of an elongated pebble within glacial
till to be aligned either parallel to or perpendicular to the

direction of ice flow if the till was deposited in association

53

with active ice. Thus, in instances where associated landforms
also bear a specific areal relationship to an active glacier
pebble alignment and landform trend may be directly related.
Possible realignment or reorientation of pebbles in glacial
till resulting from events subsequent to deposition were
reported by MacClintock and Dreimanis (1964) and by Ramsden and
Westgate (1971). In Alberta, Canada, Ramsden and.Westgate (1971)
present evidence to support a till-fabric orientation change
produced by the advance of a later glacier. Harrison (1957b)
found that the clay till fabric of the Marseilles Moraine in
northeastern Illinois (see Figure 4, in poCket) showed a
greater tendency toward perpendicular than parallel orientation
to the trend of the moraine but many fabrics appeared to have
been reoriented slightly to an unpredictable alignment. It is
worth noting at this time that the lobate form of the Marseilles
Moraine is similar to that of the Eureka-Normal Moraine (Drift).
Another study which reports the findings of till-fabric
analyses on lobate form moraines was written by Andrews and
Smithson (1965). These authors describe four morainal forms
called linear, hooked, s-shaped, and asymmetrical. The latter
is a parabolic lobate form. The results of the Andrews and
Smithson (1965) study reveal that the orientation and dip
strength in asymmetrical form moraines is poorer than the
orientation and dip strength in the other three forms. They
also concluded the orientation strength was no different from
proximal to distal lepe and that dip strength was only slightly

higher on the distal slope in asymmetrical form moraines.

54
These conclusions have special relevance to the discussion of

pebble-orientation data described later in this chapter and in

Chapters 4 and S.

Till Pebble Orientation

The horizontal long-axis orientation of a fifty-pebble
sample was determined in the field to the nearest five
degrees (see Chapter 2 for a discussion of the field technique).
Such data have been represented and analyzed in various ways.
Holmes (1941) used rose and contoured diagrams in his analysis.
Harrison (1957b) used rose diagrams and maps with preferred
orientations indicated by arrows. Krumbein (1939), Kauranne
(1960), and Andrews and Shimizu (1966) have all suggested
statistical techniques for the analysis of orientation data
but they also used orientation diagrams in these works to
show associations . In this study it was concluded that pebble
orientation could best be analyzed and compared by using rose
diagrams centered at the location of each analysis site on
a map of the study area showing the morphostratigraphic units
(See Figure 14, in pocket).

Long-axis pebble orientation for the fourteen analysis
sites in Malden Till along the Eureka-Normal Moraine (Drift)
appear consistent with the findings of both Harrison (1957b),
and Andrews and Smithson (1965). These works will be used for
cc"‘Ivaalrison in the remainder of this section as the findings

0f the till-fabric analyses of this study are reported.

55

Comparison of data from site E10 on the distal slope
with that of site Ell on the proximal slape does show the
distal orientation strength is somewhat better than the
proximal orientation strength, but the consistency of this
result is not demonstrated by the orientations at the remainder
of the analysis sites on this moraine. The tendency for long-
axis orientations to be parallel to the trend of the moraine
exists at analysis sites E8, N4, E9, and N2 but is not as
pronounced as the parallel tendency in the region near the
interlobate area at analysis sites E5, E6, and E7 (see
Figure 14, in pocket). A secondary mode orthogonal to the
primary mode is present in the orientations at analysis sites
N2 and N4. At all the remaining sites except N3, which is
trimodal, the tendency of the long-axis orientation is toward
a perpendicular to the trend of the moraine.

Both long-axis orientation and dip orientation and
strength are considered in most till-fabric studies. These
variables have a high degree of correlation and when used in
combination strengthen the fabric representation. Holmes (1941),
Harrison (1957a), West and Donner (1957), and others have
used both measurements. Dip orientation and strength will
be discussed in this study only when the rose diagram of the
long-axis orientation shows a poor or unoriented pattern.

At analysis site N3, which has a trimodal long-axis
orientation, and at analysis sites Ell, E8, and N1 where the
long-axis orientation is poor, dip orientation is considered

an alternate fabric determinant. At N3, which has little or

(n

(.1

(I)

(It

56

no orientation, there exists a moderately strong dip orientation
to the south-southeast. At N1, where there is a weak unimodal
long-axis orientation to the north-northwest, the same moderately
strong dip orientation to the south-southeast exists. The dip
orientation is moderately strong to the west at E8 and weak
to the northeast at Ell. The dip orientation shows a tendency
toward a perpendicular to the trend of the moraine except at
E8 where it tends toward a parallel alignment to the trend of
the moraine.

Figure 14 (in pocket) shows a greater tendency of fabric
orientation toward a perpendicular than parallel alignment
to the trend of the Eureka-Nermal Moraine (Drift). However,
careful examination reveals that a majority of the fabrics
show a discrepancy between a perpendicular to the trend of
the moraine and the actual pebble orientation. Harrison (1957b),
in investigating the very arcuate Marseilles Moraine (see
Figure 4, in poCket), and Andrews and Smithson (1965), in
investigating the asymmetrical form moraines on Baffin Island,
found their fabrics to be slightly askew from the perpendicular
alignment to the moraine trend they eXpected. Harrison (1957b)
suggested that these differences were the result of a till
deformation process which altered the original depositional
environment of the till. Andrews and Smithson (1965)
associated the asymmetrical form of moraines to a process of
pushing and overriding which altered and weakened the fabric
strength. If Harrison (1957b) and Andrews and Smithson (1965)

are correct regarding the relationship of the long-axis

S7
pebble orientation to the trend of a lobate form moraine, then

the data of this study supports the contention that the original
depositional environment of the pebbles in Eureka-Normal Moraine
(Drift) was altered slightly in the formation of this moraine.
As suggested by Glen, Donner, and West (1957), great care

was taken to avoid locations for analysis sites in this study
where alteration of till fabric as a result of gravitational
forces would be a factor (see Chapter 2, selection of analysis
sites). The processes by which such reorientation might take
place can only be speculated on the basis of available
information. However, it would appear that if a reorientation
did take place it is most likely that the alteration was
accomplished by a pulsation or slight readvance of the
Woodfordian ice sheet after the original formation of muCh of

the Eureka-Normal Moraine (Drift).

Till Pebble Lithology

The fifty pebbles measured for long-axis orientation
at eaCh analysis site were classified lithologically in the
laboratory. Chapter 2 contains an account of the laboratory
procedure and the resulting data can be found in the Appendix.
The purpose of the investigation of pebble lithology was to
show if a relationship exists between either pebble lithology
and morphostratigraphy or pebble lithology and rook
stratigraphy.

At this point it is appropriate to mention some of the

deficiencies of the pebble lithology analysis of this study.

58
The sample size of fifty pebbles appears too small, especially
when pebbles without a long axis were not considered.
Anderson (1955) used 100 pebbles for eaCh sample location when
studying the pebble lithology of the Marseilles Drift in
northeastern Illinois (see Figure 4, in poCket) and found a
great deal of variability both from proximal to distal side
of the moraine as well as laterally. He also found local
concentrations of particular lithologic types and his distri-
bution of sample sites was more dense than the l to 5 mile
Spacing of analysis sites for this study. In spite of these
deficiencies slight variations in pebble lithology, which
appear worthy of consideration, did exist between both
rock-stratigraphic units and morphostratigraphic units.

To accentuate these differences and facilitate analysis,
the various pebbles were grouped into lithologic categories.
The procedure involved first dividing the pebbles into
crystalline and noncrystalline groups. Then the noncrystalline
pebbles were separated into four groups: carbonate, noncarbonate
elastic, chert-flint, and other (see Chapter 2 for lithologic
types included in eaCh group).

Lithologic characteristics of Eureka-Normal Moraine
(Drift) pebbles are summarized in Table 2. Two general
conclusions can be drawn about the lithologic composition of
Eureka-Normal Moraine (Drift) pebbles in comparison to pebbles
from till associated with other morphostratigraphic units
treated in this study. First, the average number of crystalline

pebbles is very low, and, second, the average number of

59

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w m mm 4m 0H mm
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mcwflumu mxnocoz ocwdamu 930% ms." minor—4

 

 

 

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m 033.

 

60

carbonates, the majority most probably Silurian dolomites,

is very high. These conclusions were drawn after the data in
Table 2 were compared with the data in Tables 5 and 7. However,
an effective comparison of these data cannot be made until the
Characteristics of the Bloomington and Champaign Moraines
(Drifts) have been discussed. Therefore, a more detailed
discussion of pebble lithology will be presented in Chapters 4
and 5 where the lithology data for pebbles from these units

are discussed.

Congerville Section

The Congerville Section is located areally on the Eureka
Moraine (Drift) and is included in this chapter because of its
location. The importance of this stratigraphic section is
that it establishes the relationship between three‘Woodfordian
units: the Richland Loess, the Malden Till, and the Tiskilwa
Till.

Data on physical Characteristics of this section can
be found in Table 3. The upper two tills in this section
are defined as Malden and Tiskilwa Till. The data for samples
from this section are comparable to averages for samples from
analysis sites defined to have these till units. A sharp
line of demarcation between the Malden Till and Tiskilwa Till
can be found in this section. A boulder line at the base of
a thin zone of outwash clearly establishes the contact and

stratigraphic relationship of these two till members.

61

 

 

 

 

 

 

 

 

 

 

 

 

 

 

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m mHnma

 

61

 

 

 

 

 

 

 

 

 

 

 

 

 

 

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62

Congerville Section

Measured in roadcuts in NE SE NE Sec. 3, T.25 N.,
RJ1.W., Woodford County, Illinois, 1971, 1972.

Thickness
(ft)
Pleistocene Series
Wisconsinan Stage
Woodfordian Substage
Richland Loess
9. Loess; tan to tan brown, leached;
contains modern surface soil 2.0
Wedron Formation
Malden Till Member
Eureka Drift
8. Till, silty, upper part leached;
buff tan to light brown; oxidized 3.0
7. Sand and gravel, calcareous, dark
tan, shape contact boulder line at
base 0.5
Tiskilwa Till Member
6. Till, sandy, pink to red brown,
calcareous, compact angular blocky
in upper part grading to unconsolidated
near base, contains silt lenses 9.5
5. Sand and gravel, calcareous, yellow
tan 2.0
Illinoian Stage
Undifferentiated
4, Till, silty, calcareous, buff tan to tan 2.0
3. Silt, yellow tan to lemon 0.5
2. Till, silty, olive to olive tan to
pale green 1.0
l. Till, sandy, dark tan to gray to brown 9.5

 

Total 30.0

63

Long-axis pebble orientation data for the top two till
units is also included in Table 3. The fabric of the Malden
Till has a northeasterly orientation in this section and the
fabric of the Tiskilwa Till has north-northwest orientation.
The original depositional mode of Tiskilwa Till is believed
to be represented by the fabric orientation at analysis site
B15 (see Figure 14, in poCket). The long-axis pebble
orientation at analysis site EB2 shows the reorientation
effect that the glacial ice, which deposited the Eureka Drift,
had on the Tiskilwa Till in the till plain behind the
Bloomington.Moraine (Drift) (see page 88 for a more detailed
discussion).

The Woodfordian Units overlie a sequence of undifferentiated
units believed to be Illinoian in age. The important aspect
of the Congerville Section is that it clearly establishes the
stratigraphic relationship between the Tiskilwa and Malden

Till Members of this study.

Conclusions

The major conclusions of this chapter are the following:
(1) The Eureka-Normal Moraine (Drift) is one morphostratigraphic
unit. (2) Physical characteristics of the surface till within
this unit indicate that it belongs to the Malden Till Member
of the Wedron Formation. (3) Pebble orientation findings '
reveal that the long axis of elongate pebbles within this
till prefer a perpendicular alignment to the trend of the

moraine. These orientations indicate a Lake Michigan Lobe

64
source. And (4) pebble lithology data indicates that a
lower percentage of crystalline pebbles and a larger percentage
of carbonate pebbles are embedded in this till than was found
in tills from the other units of this study.

Chapter 4

CHARACTERISTICS OF THE CHAMPAIGN
MORPHOSTRATIGRAPHIC UNIT AND
ASSOCIATED INTERLOBATE AREA
Introduction

The Champaign Moraine (Drift) as delineated by Willman and
Frye (1970) was studied between the two valleys of the .
Sangamon River which are approximated by analysis site
locations Cl and C6 (see Figures 4 and 7). Near C6 the Sangamon
River Valley separates the Champaign Moraine (Drift) from the
interlobate section to the northeast, and near C1 the Sangamon
River traverses the Champaign Moraine (Drift) and separates
it into two segments.

The base of both the proximal and distal slope of the
Champaign Moraine (Drift) in the study area is clearly
defined tOpographically by the 750 foot (225 meters) contour
(see Figure 13, in pocket). However, the tapography of the
Champaign.Moraine (Drift) is more subdued than that of either
the Bloomington or Eureka-Normal Moraines (Drifts). The
distal slopes tend to be slightly steeper than the proximal
lepes but both could be categorized as gently leping to
rolling (see Figure 10). In the study area the total local
relief on the Champaign Moraine is approximately 80 feet
(24 meters), but the average relief is less than 50 feet
(15 meters) per square mile. A maximum altitude of about

830 feet (248 meters) is attained in a number of locations

65

66
between Bellflower and Saybrook (see Figure 13, in pocket).
Though the moraine is the least prominent in the study area,
it is the best defined topographically in terms of both extent
and boundaries.

Five analysis sites were selected along an 18 mile
(29 kilometers) extent of Champaign Moraine (Drift) within the
study area. Two analysis sites (C2 and C3) were in the central
part of the moraine and three (C1, C4, and C6) were on the
distal lepe (see Figure 7). The average altitude of the
exposures is 790 feet (237 meters) and the excavations average
about 11 feet (3.3 meters) below the present land surface.

The associated interlobate area of the Champaign Moraine
(Drift) is defined as the area of BD analysis-site locations,
and the criterion used to establish this area is the same
as that used to separate it from the area of BP analysis-site
locations (see page 28 and Figure 9). The base of this
area is approximated by the 750 foot contour (225 meters),
and the altitude in the central part of this region is slightly
more than 900 feet (270 meters). For purposes of discussion
and analysis, the data from the three BD analysis sites are
considered along with the data from the Champaign Meraine (Drift)
so that the relationship between the interlobate area, which
Willman and Frye (1970) refer to as Bloomington Moraine (Drift),
and the Champaign Moraine (Drift) can be established.

67
Physical Characteristics of the Till Matrix

The Erie Lobe has been divided into sublobes including
the Decatur whiCh deposited a sequence of drifts (see Figure 4,
in poCket) in east-central Illinois during the‘Woodfordian
Substage of the Wisconsinan Stage (Willman and Frye, 1970)

(see Figure 3). The Champaign Moraine (Drift) deposited by the
Decatur Sublobe is a part of the Wedron Formation rock-
stratigraphic unit that was undifferentiated by'Willman and Frye
(1970). Johnson, Gross, and Moran (1971) have studied the
previously undifferentiatedJWedron Formation in the Danville,
Illinois region and have recognized three till members that
they correlate with proposed units in the McLean County region
of the study area.

Figure 6 illustrates the relationship between the
Batestown, Unit 2, and Snider Tills. This figure also
correlates these three units with tills that were named prior
to the works in which the Batestown, Unit 2, and Snider Tills
were defined. A discussion of the physical characteristics
of the Batestown, Unit 2, and Snider Tills follows so that
their relationships to the till of the Champaign Moraine (Drift)
and associated interlobate area can be established.

The Batestown Till Member is described as a gray or dark
gray often silty till whiCh oxidizes to a characteristic
light olive brown (Johnson et al., 1972). It is known to
exist stratigraphically between the Snider and Glenburn Till
Members in the Danville region (JChnson, Gross, and Moran,
1971). Some physical Characteristics of the Batestown Till

68

Member are (l) a grain-size distribution of 28 per cent sand,
38 per cent silt, and 34 per cent clay; (2) a clay mineral
composition of 3 per cent expandable clay, 80 per cent illite,
and 17 per cent kaolinite and Chlorite; and (3) a carbonate
content of 5 per cent calcite and 19 per cent dolomite
(Johnson, Gross, and Moran, 1971; and.Johnson et al., 1972).

Unit 2 is described as a gray silty till, but a pinkish
tint has been noted in some samples on the outer margin of the
till (Kempton, DuMontelle, and Glass, 1971). The averages
for 150 samples of Unit 2 till showed (1) a grain-size
distribution of 27 per cent sand, 45 per cent silt, and
28 per cent clay; (2) a clay mineral composition of 3 per cent
montmorillonite (see footnote 5, page 48), 79 per cent illite,
and 18 per cent chlorite and kaolinite; and (3) a carbonate
content of 14 counts per second calcite and 21 counts per second
dolomite (Kempton, DuMontelle, and Glass, 1971).

The Snider Till Member is a gray brown to light olive brown
till where oxidized and a dark gray where unoxidized
(JChnson, Gross, and Moran, 1971). In comparison with the
Batestown Till it contains less sand and slightly more illite
(JChnson, Gross, and Moran, 1971; Johnson et al., 1972).
JChnson, Gross, and Meran (1971) reported the average physical
characteristics of the Snider Till Member to be (1) grain-size
distribution 19 per cent sand, 45 per cent silt, and 36 per cent
clay; (2) clay mineral composition 3 per cent expandables,
85 per cent illite, and 12 per cent kaolinite and Chlorite; and

(3) carbonate content 6 per cent calcite and 19 per cent dolomite.

69

With some of the physical characteristics of the Batestown,
Unit 2, and Snider Tills established, a discussion of the data
provided by analyses of till-matrix samples from the Champaign
Meraine (Drift) and the associated interlobate area may be
presented. These data are contained in the Appendix and
summarized in Table 4. Averages for the BD locations and C
locations are figured separately so that they may be compared.
The data in the table are arranged in order from north to south
along the trend of the moraine (see Figure 7).

Till samples from analysis sites C2 and C4 were from a
depth of 15 feet (4.5 meters) and were an unoxidized gray.
The till-matrix samples from locations Cl and C3 came from
a depth of 9 feet (2.7 meters) and 5 feet (1.5 meters)
respectively. Their colors were a greenish gray to olive gray,
the Characteristic oxidation colors for both the Snider and
Batestown Till Members (JChnson et al., 1972). All the
remaining samples listed in Table 4 came from shallow depth
analysis sites, (see the Appendix for depths) were oxidized
but calcareous, and have a tan color.

Comparison of the physical characteristics of the till
samples of Champaign Moraine (Drift) with those from the
BD locations in the interlobate area reveal no major
consistent differences. From the numerical data in Table 4,
it can be concluded that the till from BD locations on the
interlobate and till from the analysis sites on the Champaign

Moraine (Drift) are the same till.

7O

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omumfixo ococ use ouHono pom nmu>Hmcm

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

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cowumcfixo wo museums wzowpm> ou >HHomEHno one 4
mH m «H 4m 4 an 04 mm 4\msm.m nm.m>a
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acoucou mumcooumo cowuwmooeoo Hmuocfiz amHu coHusoHpUmHm CNHm :Hmpo .Hmca

 

 

 

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--xHeumz HHHe men to moHumHeeuememeo HeeHmsae

4 eHeea

 

71

A comparison of the numerical data for physical
characteristics of the Batestown Till Member and its correla-
tive Unit 2 with the numerical data of Table 4 reveals two
differences: (1) the Batestown Till and Unit 2 have a
slightly sandier texture, and (2) the Batestown Till and Unit 2
have a little less illite. However, these differences are
the same differences that separate the Batestown Till Member
from the Snider Till wither. On this basis a correlation,
though somewhat uncertain, may be drawn between the Snider Till
Member and the various till samples whose physical
characteristics are summarized in Table 4. This correlation
of numerical data is strong enough that it can be concluded
that the till on the Decatur Sublobe side of the Bloomington
interlobate (see Figure 9) and the till of the Champaign Moraine
(Drift) in the study area of this thesis are a part of the
Snider Till Member of the Wedron Formation rock-stratigraphic
unit. This conclusion is not inconsistent with the correlation
drawn by Johnson, Gross, and Moran (1971), who correlated the
Batestown Till with both Unit 2 and upper till in the Champaign-
Urbana region of Kempton, DuMontelle, and Glass (1971), because
the latter authors did not define the till in the section of
Champaign Moraine (Drift) studied in this thesis. The
correlation between the till described in Table 4 and the
Batestown Till still remains a possibility on the basis of
data from analysis sites BBB, C6, and Cl because of the sandier
texture of the till at these locations. However, the high

illite content in the clay mineral fraction at BBB and C6

72
agree with the Snider Till correlation. Therefore, the till
samples from analysis site C1 are the only ones which might be
correlated with the Batestown Till. These findings are not
inconsistent with the findings of Willman and Frye (1970)
because the till of the Champaign Moraine (Drift) was not
differentiated by them and because there still remains the
possibility that the Malden Till Member, to which they assigned
the interlobate region, can be correlated with the Snider Till
Member (this correlation will be suggested later in this
study).

Characteristics of Till Pebbles
Introduction

The purpose of this section is to discuss and analyze
first, the relationships between long-axis pebble orientation,
and both rock stratigraphy and morphostratigraphy; and,
second, the relationShips between the lithologic composition
of pebbles and both rock stratigraphy and morphostratigraphy.

Data on pebble orientation, lithology, size, and shape
for a fifty-pebble sample from eaCh analysis site on the
Champaign Moraine (Drift) and from each BD analysis site
in the associated interlobate area can be found in the Appendix.

Data on pebble size and shape were not analyzed in this study.

Till Pebble Orientation
Long-axis pebble orientation data for the analysis sites
along the Champaign Moraine (Drift) and the BD locations in

the associated interlobate region are illustrated on

 

73

Figure 14 (in pocket). Analysis sites C1, C4, and C6 are
located on the distal side of the moraine while C2 and C3
are near the crest. The three analysis sites in the associated
interlobate region would be on the proximal slope if this
till was deposited by the Decatur Sublobe. However, Willman
and Frye (1970) have mapped the drift of this segment as
having been deposited by the Peoria Sublobe which, if correct,
would place the analysis sites on the distal side of the
Bloomington Moraine (Drift). Regardless of the interpretation
selected, assuming Andrews and Smithson (1965) are correct,
the position of analysis site with respect to the outline of the
moraine makes very little difference in pebble orientation
strength when asymmetrical (parabolic-lobate) form moraines
are being considered. Therefore, the pebble orientation
data from both the Champaign Moraine (Drift) and associated
interlobate area will be discussed together and consideration
of location with respect to outline of the moraine will not
be included in a discussion of the interlobate area orientations.

Reasonably strong long-axis orientation patterns exist
at seven of the eight locations studied (see Figure 14,
in pocket). The one exception is at analysis site C1 where
the long-axis orientation is bimodal and weak. The alternate
measurement of dip strength is strong to the southwest for
this location. SuCh an orientation at location Cl tends
perpendicular to the trend of the moraine. The tendency towards
a long-axis pebble orientation which is orthogonal to the

trend of the moraine is more prevalent along the Champaign

74
Moraine (Drift) than along the Eureka-Normal Moraine (Drift)
previously described. In the associated interlobate section,
however, the tendency of the primary pebble fabric is to
become parallel to the morainal unit with the secondary mode
tending toward the perpendicular. This important relationship
is also shown in the interlobate area associated with the
Bloomington Moraine (Drift) and is elaborated upon in Chapters
5 and 6. Comparison of the actual long-axis pebble orientations
as represented by the rose diagrams on Figure 14 (in pocket)
with the true perpendicular to the trend of the moraine once
again reveals a discrepancy. The orientations are slightly
askew from a true perpendicular indicating, as was the case
with the Eureka-NOrmal Moraine (Drift), that a pulsation or
readvance of a retreating ice sheet may have reoriented the
fabrics slightly from.their original depositional environment.
This possibility is based on the long-axis orientation findings
of this study and the previous work of Harrison (1957b)
and Andrews and Smithson (1965).

Till Pebble Lithology
The lithologic classification of each pebble from

analysis sites along the Champaign Moraine (Drift) and the

BD locations of the interlobate area can be found in the
Appendix. These data are categorized and summarized in

Table 5. A comparison of the data for C locations with the
data for ED locations reveals a small difference in percentage
of crystallines and a slightly larger difference for percentage

of noncarbonate clastics. The latter difference can be

75

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

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76
attributed to a local concentration of shale pebbles in the
area of the interlobate. Anderson (1955) believes that the
sedimentary parameter of pebble lithology can be used to
distinguish deposits from different lobes. Within the study
area the only discernible differences in pebble lithology
between the samples from the Peoria and Decatur Sublobes are
reflected by the 9 per cent difference in carbonates. It
appears that when the sample size is large (700 Eureka-Normal
pebbles versus 400 Champaign-BB pebbles) that this degree of
variation may be significant enough to provide a baSis for

determining primary source.

Conclusions

The major conclusions of this Chapter are the following:
(1) The till within the Champaign Meraine (Drift) and the
till within the associated interlobate area are both correlated
with the rock-stratigraphic unit named the Snider Till Member
of the Wedron Formation. (2) The long-axis pebble orientations
of the Champaign Moraine (Drift) tend to be orthogonal to the
trend of the morphostratigraphic unit outside of the interlobate
then become parallel to the landform in this area. These
orientations indicate an Erie Lobe source for this till. And
(3) the pebble lithology data from the Champaign Moraine (Drift)
and associated interlobate indicate that pebbles within till
from an Erie Lobe source have approximately 9 per cent fewer
carbonate pebbles than pebbles within till from.a Lake MiChigan

Lobe source.

Chapter 5

CHARACTERISTICS OF THE
BLOOMINGTON MORPHOSTRATIGRAPHIC UNIT
AND ASSOCIATED INTERLOBATE AREA
Introduction

The Bloomington Moraine (Drift) as defined by'Willman
and Frye (1970) was studied from the TazewellqMCLean County
line on the west to the interlobate area just east of the
Ford-McLean County line on the east (see Figure 4, in pocket).
This section of the Bloomington Moraine (Drift) has the most
massive topOgraphic form of any of the morphostratigraphic
units under consideration in this study (see Figure 13,
in pocket). The local relief repeatedly exceeds 100 feet
(30 meters) and the moraine varies in width from 1.5 to
4.5 miles (2.4 to 7.2 kilometers). The areal plan of the
Bloomington Moraine (Drift) does not show the consistent
arcuate lobate form that is exhibited by the Eureka-Normal and
Champaign Moraines (Drifts) (see Figure 4, in pocket).

TOpographically, it can be divided into three sections:
(1) a section west of Bloomington, Illinois, which has its own
small lobate form; (2) a central section which is almost
linear in form; and (3) an interlobate section which has a
form similar to the other moraines that merge to form this
area. The western section is separated from the central section
by the valley of the Sugar Creek (see Figure 13, in poCket).
This western section has a distal base whiCh is approximated

77

78
by the 750 foot (225 meters) contour and a maximum altitude
of 883 feet (265 meters). The central section is separated
from the interlobate section by the valley of the Sangamon
River. The central section has a distal base of approximately
800 feet (243 meters), and crest altitudes of over 900 feet
(265 meters) are common in this part of the Bloomington.Moraine
(Drift) giving it a massive and prominent appearance (see
Figure 13, in pocket). Here the proximal slopes are more
gently rolling than the steeper distal slapes due in part to
the higher altitude of the proximal base. This base is some-
what variable but generally parallels the 800 to 850 foot
(243 to 265 meters) contour depending on location. The third
section is the associated interlobate area of the Bloomington
Moraine (Drift). This section is defined by the BP analysis
site locations and the areal extent is illustrated on Figure 9.
The base of this area is approximately 825 feet (260 meters)
and the crest altitude exceeds 900 feet (265 meters).

At four places stream erosion has resulted in extreme
dissection of the Bloomington.Moraine (Drift) (see Figure 13,
in pocket). Sugar Creek, Kickapoo Creek, and the Sangamon
River traverse the Bloomington Moraine (Drift) while the
North Fork of Salt Creek partially dissects this same moraine.
The topography near their associated valleys is more rugged
and very steep slopes are common (see Figure 10).

Fifteen analysis sites were selected for the purpose
of collecting samples from the Bloomington Moraine (Drift)

(see Figure 7). Two sites were on the proximal slope, four

79

were in the central area near the crest, five were on the
distal slope, and four were situated along the west flank of
the interlobate section (see the Appendix for specific
locations). Average depth of analysis below the t0p of the
soil profile was approximately 9 feet (3 meters) with excava-
tions ranging from 4 feet (1.3 meters) to 25 feet (7.5 meters)
below the surface of the Bloomington Moraine (Drift). The
surface of this drift above the analysis sites had an average
altitude of 834 feet (250 meters). Data on physical
characteristics of the till matrix, long-axis pebble orienta-
tion, and the lithology of pebbles collected from the fifteen
analysis sites on the Bloomington Moraine (Drift) are contained
in the Appendix. These data will be compiled, summarized, and
presented in this chapter so that the basic question of relation-
ships between morphostratigraphy, roCk stratigraphy, pebble
lithology, and pebble orientation can be answered.

Physical Characteristics of the Till Matrix

The Bloomington Moraine (Drift) in the study area of this
thesis does not have the consistency found in the Eureka-Normal
and Champaign Moraines (Drifts). Both Willman and Frye (1970)
and Kempton, DuMontelle, and Glass (1971) recognized two till
units in this part of the study area. Willman and Frye (1970)
mapped the till on the Bloomington Moraine (Drift) west of
Bloomington, Illinois, as belonging to the Tiskilwa Till Member
and the till east of that same city as a part of the Malden
Till Member (see Figure 5). The latter authors describe the
till on the Bloomington Moraine (Drift) in McLean County to

 

80
the west of Danvers,6 Illinois, as Unit 4 Till and the till in
McLean County to the east of the Danvers area as Unit 2 Till.
These authors also postulated and mapped a third till named
Unit 1 overlying the proximal slope of this moraine in places.
The Malden Till and Unit 1 were previously described in
Chapter 3, and Unit 2 was described in Chapter 4.

The Tiskilwa Till was described by’Willman and Frye (1970)
as a sandy, pink tan to reddish tan brown till (usually called
pink) that is overlain by the Malden Till and may rest on the
Delavan, Esmond, or Lee Center Till Members. Some of the
physical characteristics of the Tiskilwa Till Member are
represented by data from two samples of Bloomington Moraine
(Drift) reported.by Willman and Frye (1970) to contain this
unit. Averages show (1) a grain-size distribution of
approximately 29 per cent sand, 37 per cent silt, and
34 per cent clay; (2) a clay mineral composition of 18 per cent
expandable clays, 68 per cent illite, and 14 per cent kaolinite
and chlorite; and (3) a carbonate composition of 23 counts per
second calcite and 36 counts per second dolomite. Kempton,
DuMontelle, and Glass (1971) gave the following description
of Unit 4 Till in McLean County:

It is normally a reddish brown to pinkish gray till.

Locally, this till grades to brownish gray. It can

nearly always be differentiated from the upper three

units in the region on the basis of color and clay

mineral composition, particularly when one or more

of the upper units are found in sequence with Unit 4.
This till unit is slightly silty, averaging 30 per cent

 

6The location of Danvers is approximated by analysis
site B5 on Figure 7.

81

sand, 40 per cent silt, and 30 per cent clay.

The average clay mineral content is 8 per cent

montmorillonite, 70 per cent illite, and 22 per cent

Chlorite plus kaolinite. No significant change in

clay mineral composition or grain size of the unit

occurs with changes in color. Unit 4 contains the

greatest amount of carbonate of all five units.

Numerical data describing certain physical characteristics
of the till matrix for the fifteen analysis sites on the
Bloomington Moraine (Drift) are summarized.in Table 6 and
arranged in this table in order from east to west along the
trend of the moraine (see Figure 7). Because previous workers
have recognized more than one rook-stratigraphic unit within
the Bloomington Moraine (Drift) (Willman and Frye, 1970;
Kempton, DuMontelle, and Glass, 1971), it may be more
revealing if the samples are divided into as many groups as is
meaningful on the basis of available data. The result is the
recognition of three distinct till units within this part of
the study area. For purposes of this discussion these are
named Units A, B, and c to avoid confusion with the Kempton,
DuMontelle, and Glass number system. Unit A is defined on the
basis of data for till samples from analysis sites 813, B14,
BS, and 815 (east to west); Unit B by till samples from sites
B4 and B3; and Unit C by till samples from all the remaining
analysis site locations whose data is summarized in Table 6
(see Figure 7 for locations).

Comparison of the averages of Unit A data reported in
Table 6 with the average numerical physical Characteristic
data of the Tiskilwa Till Member (Willman and Frye, 1970)

and also Unit 4 (Kempton, DuMontelle, and Glass, 1971) reveals

82

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83
a high degree of similarity. This is especially well shown

when comparing the low illite content, high carbonate content,
and pink color. On this basis it is reasonable to conclude that
the surface till on the Bloomington Morphostratigraphic Unit
to the west of the city of Bloomington belongs to the Tiskilwa
Till Member of the Wedron Formation rook-stratigraphic unit.
This correlation is commensurate with the mapping of this unit
by Willman and Frye (1970), but does not agree with the tenta-
tive boundary drawn between Unit 2 and Unit 4 by Kempton,
DuMontelle, and Glass (1971). The findings of this study
would suggest that this tentative boundary of Kempton,
DuMontelle, and Glass (1971) be placed near the KiCkapoo Creek
Valley and that the distribution of Unit 1 till be restricted
to the proximal slape of the Bloomington Moraine (Drift).

Unit B, the second of the three groups under discussion,
can be differentiated from Units A and C on the basis of
color and clay mineral composition. This unit is violet gray
when unoxidized and a gray brown or tan when oxidized. The
clay mineral composition of this unit has less expandable
clay than Unit A and less illite than Unit C, producing a
greater percentage of Chlorite and kaolinite than either of
the other units. Less significant differences exist in both
texture, Unit B a little sandier than both Units A and C,
and carbonate content, slightly more calcite in Unit B than
Unit A and a great deal more calcite in Unit B than Unit C
(see Table 6). Willman and Frye (1970) included the area
defined by analysis sites B3 and B4 in the Malden Till Member,

84

but findings of this study indicate that Unit B is clearly
different from.the Malden Till. Furthermore, Unit B cannot

be correlated with Unit 4 Till, which was recognized and mapped
in this area by Kempton, DuMontelle, and Glass (1971), because
the differences between Unit B and Unit 4 Till are the same as
the differences already described between Unit B and Unit A

of this study. Thus, in the Opinion of the author, Unit B
should be treated as a separate and distinct till that has not
been correctly correlated with any other rock-stratigraphic
unit to this date. It should be pointed out, however, that the
conclusion that Unit B Till has not been defined by previous
investigators is based on the physical Characteristic data
from.two analysis sites. Because data from only two sample
sites may be judged insufficient for the purpose of naming a
new till member, additional data were gathered from drill borings
in.McLean County. Data from drill borings McLean 10, 12, l3,
17, 18, 20, 21, and 25 support and extend the existence of this
till unit. Figure 15 gives the location and elevation of these
drill borings. At each of these drill-boring locations
analyses of the clay fraction of split spoon samples reveal

the existence of a till which is violet gray in color and has

a clay mineral composition of approximately 7 per cent expandable
clay, 70 per cent illite, and 23 per cent chlorite plus
kaolinite. These data are on file in the geologic records
section of the Illinois State Geological Survey in Urbana,
Illinois. With the addition of this evidence the author

85
pr0poses that Unit B be hereafter referred to as the Shamrock

Till Member of the Wedron Formation. The suggested name is
for the town of ShamroCk in MoLean County. The type section
is an exposure in a borrow pit (see Figure 8B) on the north
side of I-74 1.5 miles (2.4 kilometers) west of Shamrock,

SE SE SW, Sec. 25, T.23 N., R.2 E. The name Shamrock Till
will be used in the remainder of this paper to refer to Unit B
Till, and the type section will be described later in this

 

 

 

 

 

 

 

 

 

chapter.
McLean No. Location Elevation
10 NW SE Sec.22 T.23 N. R.2 E. 785
12 SE SE NW Sec.26 T.23 N. Rm2 E. 849
13 NE NW Sec.36 T.23 N. R.2 E. 803
17 NW SW NE Sec.33 T.24 N. Rm2 E. 774
18 SW NW NW Sec.5 T.23 N. R.2 E. 730
20 SE NW Sec.5 T.22 N. R.3 E. 747
21 NW NW Sec.5 T.22 N. R.3 E. 784
25 SE NW Sec.5 T.22 N. R.3 E. 748

 

 

 

 

 

Figure 15 McLean County drill boring locations

Unit C Till has very different physical Characteristics
from either Unit A or Unit B Till. The most noticeable
differences are (l) finer texture, (2) high illite content,
and (3) fewer carbonates. The averages reported in Table 6
for Unit C are from sample sites within both the Bloomington

Moraine (Drift) and the associated interlobate area. The data

86

in Table 6 indicates that the till samples from all analysis
sites included in the Unit C group probably belongs to the same
rock-stratigraphic unit. Comparisons of the numerical averages
which represent the physical Characteristics of Unit C Till
described in the area shows that a strong similarity exists
between Unit C Till and Malden Till. On the basis of this
similarity it is probable that a correlation exists between
Unit C and the Malden Till. This interpretation is consistent
with the findings of Willman and Frye (1970). Kempton,
DuMontelle, and Glass (1971) separated the Malden Till in the
study area of this thesis into Units 1 and 2 mainly on the
basis of texture. The results of the till-matrix investi-
gations for this thesis do not provide a basis for the
separation of the Malden Till into two units. There are some
locally sandy places in the Unit C group, but, in the opinion
of the author, the relatively small differences in texture do
not provide an adequate basis for the recognition of more than
one till member. Therefore, it is concluded that the till in
Unit C is the equivalent of the Malden Till and is referred

to as such in the remainder of this study.

Characteristics of Till Pebbles
Introduction
The purpose of this section is to present the data on
long-axis pebble orientation and pebble lithology for
750 pebbles from analysis sites associated with Bloomington
Moraine (Drift) (Willman and Frye, 1970). Orientation and

87
lithologic data are contained in the Appendix and are

summarized in Figure 14 (in poCket) and Table 7 respectively.
The discussion of these data will be directed toward a clearer
understanding of the relationship between the sedimentary
parameter and associated landform unit.

Till Pebble Orientation

Due to the complexity in.morphostratigraphic and
roCk-stratigraphic units within the Bloomington Moraine
(Drift), long-axis pebble orientation data will be discussed
in association with Units A, B, and C as previously described
because a definite relationship can be shown to exist. The
fabric orientations of pebbles measured in Unit A Till
(Tiskilwa Till) exhibit a consistent tendency toward a
perpendicular alignment to the trend of the moraine (see
Figure 14, in poCket). The strong north-south alignment of
pebbles at analysis site 315 probably best represents the
original depositional mode of Tiskilwa Till because the Malden
Till does not overlie the proximal slope of the moraine in this
area. However, it appears likely that the till at locations
BS, B13, and 814 may have been deformed slightly by ice that
eventually constructed the Eureka-Normal Moraine (Drift)
because Kempton, DuMontelle, and Glass (1971) report Unit 1
Till on the proximal slope of the Bloomington Moraine (Drift)
in this area.

The Congerville Section previously described in Chapter 3
shows an exposure of Tiskilwa Till stratigraphically below

88
the Malden Till. Pebble-orientation data from analysis site
EB2 (see Figure 14, in pocket) reveal that a slight
reorientation may have occurred in the ground moraine deposited
in association with the Bloomington Moraine (Drift). The
slight reorientation is illustrated by comparing the rose
diagram associated with the pebble alignment at EB2 with the
comparable diagram for B15 (see Figure 14, in pocket). A
probable cause for this slight realignment is believed to be
a result of subsequent ice movement that deposited the Malden
Till.

Within the Bloomington Moraine (Drift) the ShamroCk Till
(Unit B), represented by analysis sites B3 and B4, can be
separated topographically from.the Tiskilwa Till on the west
by the valley of the Sugar Creek, and from the Malden Till
on the east by the valley of the KiCkapoo Creek. These
boundaries extend topographically to the south and incorporate
parts of the Shirley and LeRoy Drifts (see Figures 4 and 13,
in poCket). Data from drill boring MCLean 17 (see Figure 15
for location) indicate that the ShamroCk Till is stratigraphic—
ally overlain by the younger Malden Till and probably rests
upon the older Tiskilwa Till in the subsurface. The long-axis
pebble orientation data from ShamroCk Till at analysis site B4
is the strongest orientation discovered in this study. Fifty-six
per cent of the pebbles were oriented in a 30 degree sector
around east-west and dip strength is to the east. Analysis
site B3 from the same till also has an east-west fabric

orientation with 28 per cent in the same eastawest sector.

89
This strong eastHwest orientation of pebbles in Shamrock Till

is clearly at variance to other nearby sites and suggests it
formed in association with westwardsmoving ice. If this con-
clusion is correct, it is reasonable to suggest that the source
of the ShamroCk Till may well be from the Erie rather than the
Lake Michigan Lobe. The Erie Lobe source for Shamrock Till
is postulated under the assumption that certain pebbles tend
to align themselves parallel to the direction of ice move-
ment (RiChter, 1932; Cailleux, 1938, and Lundquist, 1949),
and supported by the fact that the Shamrock Till is unlike the
drift in this area deposited by the Lake Michigan Lobe. How-
ever, because of the limited data and complexity of the drift,
it is recommended that additional study be initiated regarding
the Shamrock Till so that the conclusion of an Erie Lobe
source for this till can be definitely confirmed or rejected.
Fabric orientations in Unit C (Malden Till) on the
Bloomington Moraine (Drift) show’a high degree of similarity
to the fabrics of the Eureka-Normal Moraine (Drift) to the
north, which has also been classified in this paper as Malden
Till (see Chapter 3 and, Figure 14, in poCket). Strong
perpendicular orientations to the trend of the moraine are
found at analysis sites 81, 86, and B12. Locations 81 and 86
are on the proximal side of the moraine and 812 is near the
crest. Unimodal but weak fabric orientations were found at
analysis sites 82 and 89 both near the crest of the moraine.

Dip strength, an alternate measure of orientation, is to the

90
south at B9 and to the southeast at 82, giving both fabrics

a weak preferred orthogonal alignment to the morainal trend.
The interlobate analysis sites on the Peoria Sublobe
side of the interlobate section (see Figure 9) show a
tendency toward a parallel alignment of pebble axis to trend
of the topography. This tendency for pebbles to align them-
selves parallel to the landform is illustrated by the fabric
diagrams at most BD and BP analysis sites as well as at the
three E locations near the interlobate region (see Figure 14,
in pocket) and is especially worthy of attention and
explanation. Parallel alignment of pebble axis to landform
trend is not unusual. The fabric of sediments associated with
a drumlin often reveal such a relationship. Wright (1957),
in his studies of drumlins in Minnesota, reports that almost
all rose diagrams representing pebble alignment show a strong
preference toward a parallel alignment*with the landform trend.
Glen, Donner, and.West (1957) conclude that the mechanisms by
which stones become oriented in till are most favorable to an
alignment parallel to the direction of ice flow. Data from
this study indicates that the long axis of pebbles prefer
an orthogonal arrangement to the end moraine outside the
interlobate area but Changes to a tangental arrangement in
the interlobate area. If Glen, Donner, and.West (1957) are
correct, then the pebble orientation data outside the inter-
lobate area indicates ice flow perpendicular to the end moraine
and the pebble orientation data in the interlobate area

indicates that the ice flow associated with an interlobate

91
landform is moving parallel to the ice-contact zone. It is
reasonable to assume that the pressures produced at the
contact between two glacial ice lobes could force the ice and
its associated sediments to flow parallel to the contact zone.
Therefore, it is a conclusion of this study that the sedimentary
parameter data of pebble orientation may reveal the nature of
ice behavior in an interlobate moraine and that the till fabric
in areas believed to be interlobate landforms could possibly

be identified using the data of this parameter.

Till Pebble Lithology

Table 7 contains a summary of the lithologic classifi-
cation of pebbles from all B and BP analySis sites. The
original data can be found in the Appendix. A discussion of
the limitations in the use of this data and a discussion on
the lithologic categories used in this analysis can be found
in Chapter 2. In this section an attempt will be made to
analyze and compare the data in Table 7 with the data in
Tables 2 and 5. Results for data on lithologic composition
of pebbles in Tables 2, S, and 7 are not consistent.
Crystalline percentages are highly variable between analysis
sites. The same is true of noncarbonate clastic percentages.
The only patterns that have become apparent in the study of
pebble lithology for all units in the study area are these:
(1) the percentage of carbonate pebbles for the entire inter-
lobate area and the Champaign Moraine (Drift) is consistently
low; and (2) the percentage of chert and flint pebbles in the

92

 

 

 

 

 

 

 

 

 

 

 

 

 

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93

entire interlobate area and Champaign Moraine (Drift) is
slightly higher than the comparable percentages for Eureka-
Normal Moraine (Drift) pebbles and nearly double the percentage
of chert and flint pebbles found in the Bloomington Mbraine
(Drift) exclusive of its associated interlobate analysis sites.
A comparison of lithologic composition between all
interlobate analysis site locations (see Figure 9) reveals
very little variation. The same is true in a comparison of
the lithologic composition of pebbles from the C analysis
sites with pebbles from both the BP and BD locations. Based on
the data provided by analysis of the lithologic composition of
elongate pebbles, it appears that the interlobate area of this
study has a higher degree of similarity to the Champaign
Meraine (Drift) (Snider Till) than to any other unit. However,
the till-matrix composition data and pebble orientation data
from.the till within the interlobate area indicate the following:
(1) The till found in the interlobate area associated with the
Bloomington Moraine (Drift) (Malden Till) and the Champaign
Meraine (Drift) (Snider Till) are very similar (see Tables 2
and 5); and (2) the pebble orientations within the till of
the interlobate area indicate that the Malden and Snider Tills
were probably deposited contemporaneously. Therefore, based
on all the appropriate data, it is suggested that the landform
defined in this study as the interlobate area, which was
defined by Willman and Frye (1970) as Bloomington Drift, be
named the Champaign-Bloomington Interlobate Moraine (Drift).

94

Shamrock Section
The ShamroCk Section is the type section for a new
suggested till member defined in this study. Analysis site
34 on Figure 7 marks the location of this section, and

Figure 88 is a photo of the exposure. A description of this

section follows.

Shamrock Section

Measured in a borrow pit in SE SE SW Sec. 25, T.23 N.,
R.2 E., McLean County, Illinois, 1971, 1972.

 

Thickness
(ft)
Pleistocene Series
Wisconsinan Stage
Woodfordian Substage
Richland Loess
2. Loess; thin layer of tan to tan brown to black
loess, locally coarse textured, leached modern
surface soil grades into unit one below 2.5
Shamrock Till Member (type section)
1. Till, tan to gray brown in upper part where
oxidized to violet gray where unoxidized
in lower part, compact angular blocky, silty
till zones with very few pebbles irregularly
spaced in profile 14.5
Total 17.0

The Shamrock Till physical characteristics are (l) a
grain-size distribution of 30 per cent sand, 38 per cent silt,
and 32 per cent clay; (2) a clay mineral composition of
7 per cent expandable clays, 70 per cent illite, and 23 per cent
Chlorite and kaolinite; and (3) a carbonate content of 18 counts
Per second calcite and 30 counts per second dolomite. Drill
boring McLean 17 (raw 9» NE Sec. 33, T.24 N., R.2 e.) to the

95
north of the type section shows the stratigraphic position of

the Shamrock Till as between the older Tiskilwa Till and the
younger Malden Till. Kempton, DuMontelle, and Glass (1971)
map the area defined in this study to have Shamrock Till as
Unit 4 Till, which is correlated with the Tiskilwa Till. The
ShamroCk Till can be differentiated from the Tiskilwa and Unit 4
Till on the basis of color and clay mineral composition. The
Shamrock Till is a tan or yellow tan till when oxidized and
a gray or violet gray when unoxidized with the zone of
oxidation at approximately 13 feet (4 meters) in the type
section. The Tiskilwa Till has a salmon or peach color when
oxidized and is pink to red brown where unoxidized. An
easily discernible difference in clay mineral content separates
these two units. The Shamrock Till has an average of

10 per cent less expandable clay than the Tiskilwa Till, and
this difference is nearly balanced by the 8 per cent greater
chlorite plus kaolinite content found in the Shamrock Till.
In the Kempton, DuMontelle, and Glass (1971) paper these
variables were not considered. Only illite content was
considered, which is approximately the same for both the
Shamrock and Unit 4 Tills. These differences clearly
estatflish.the necessity for defining a new till member. The
till fabric data in the area of this type section confirm the
need for a new unit. The long-axis pebble orientation data
of this study indicate that the Shamrock Till could possibly

have come from an Brie Lobe source because the fabric has a

96
strong east-west orientation in the type section. The
topography to the south of this type section indicates the
possibility of a north-south trending landform which, if it
did contain Shamrock Till, would strengthen the Erie Lobe
source hypothesis. Analysis of the till and till fabric to the
south of the Shamrock Till of this study is suggested for
future investigation. The significance of the ShamroCk
Section is that it represents a significant exposure of till
from the Bloomington.Moraine (Drift) not previously defined.

Conclusions

The major conclusions of this chapter are the following:
(1) The Bloomington Moraine (Drift) has three distinct surface
tills in the study area: the Tiskilwa, Malden, and Shamrock
Till Members. The latter was named and defined in this chapter.
(2) Pebble-orientation data indicate that elongate pebbles
prefer a perpendicular alignment to the moraine trend outside
of the interlobate area but a parallel alignment to the landform
is preferred in the interlobate area. And (3) the data of
this study indicate that the interlobate area should be
named the Champaign-Bloomington Interlobate Moraine (Drift).

Chapter 6

CONCLUSIONS AND IMPLICATIONS

Introduction

 

The purpose of this thesis is to establish the relation-
ships that exist between certain sedimentary parameters of
glacial till and particular glacial landforms. The sedimentary
parameters investigated were long-axis pebble orientation,
pebble lithology, and matrix composition. The glacial land-
forms studied were end moraines which represent recognized
morphostratigraphic units. Two of the end moraines
investigated merged into an interlobate moraine. Figure 16
summarizes the relationships between.morphostratigraphic and
rock-stratigraphic units established by this study. Also
illustrated on this map is direction of ice flow as indicated
by pebble-orientation data. Implications of the specific

findings of this study have general application in geomorphology.

General Implications
The morphostratigraphic units of this study represent
one interpretation of the glacial landforms in central Illinois
that have been delineated mainly on the basis of tapographic
expression (see Figures 4 and 13, in pocket). Findings of this
study indicate that morphostratigraphic units clearly exist,
but a reevaluation of their forms and sedimentary associations

may make them even.more useful and meaningful as geomorphic

97

98

 

 

l..________

<0 J MCLEAN
0’

 

 

MALDEN TILL

[U] SNIDER TILL

[E SNIDER-MALDEN TILL

[E] TISKILWA TILL

LIE SHAMROCK TILL 0:13 P gowns

I ICE FLOW 0 5 IOKM
CT'E—‘T—ITD

 

Figure 16 Relationships between morphostratigraphic
units,.rock stratigraphic units, and ice
flow in the study area

 

99
units. Such reassessments were a major objective of this study,
and the following are examples of findings or problems that
have been recognized as a result: (1) the reinterpretation of
the Eureka-Normal relationship as discussed in Chapter 3,
(2) the variation in till associated with the Bloomington
Moraine (Drift) which calls for a reassessment of that
morphostratigraphic unit as discussed in Chapter 5 and to be
discussed later in this chapter, and (3) the complexity and
interrelationship within the interlobate area between the
Bloomington and Champaign Moraines (Drifts) that indicate it
was formed in association with an Erie-Lake Michigan Lobe
ice contact as discussed in Chapters 4 and 5.

It is also important to recognize that certain problems
are associated with any attempt to show relationships between
morphostratigraphic units and sedimentary parameters. If two
or more morphostratigraphic units merge, it may be impossible
to understand their relationships without sedimentary parameter
data and even that information may be insufficient for a
reasonable interpretation. This problem is just one of the
many difficulties that will present itself in studies that
attempt to relate morphostratigraphy with associated sediments.
However, the morphostratigraphic unit can be a very useful and
meaningful unit when carefully mapped. The Champaign.Moraine
(Drift) of this study is a good example. This unit is easily
delineated by its tapographic eXpression. The surface till
throughout its extent is a part of the same rock-stratigraphic

unit. And the fabric complements its shape and depositional

100
mode. This situation demonstrates that it is possible to define

morphostratigraphic units which have positive relationships
to their sediments and related fabrics.

Evaluation of the relationships between morphostrati-
graphic and rock-stratigraphic units, which is one of the stated
purposes of this thesis, has revealed evidence that supports
a reinterpretation of the morphostratigraphy of central
Illinois. A proposed alternate interpretation of the
morphostratigraphy in central Illinois is a major conclusion

of this study and is discussed below.

An Alternate Interpretation of the
Morphostratigraphy in Central Illinois

Figure 16 illustrates the relationship between
morphostratigraphic units and the defined or correlated till
members of this study. Ice-flow direction, which is suggested
by the preferred long-axis orientation of each till member,
is indicated with arrows on this map. A congruent relation-
ship exists between the Bureka-Normal Moraine (Drift) and the
Malden Till and also between the Champaign Moraine (Drift) and
the Snider Till. Pebble-orientation data indicate that ice
flow reflects a direct relationship to these and moraines.
However, the relationships between the morphostratigraphic
unit, rock-stratigraphic units, and ice flow for the
Bloomington Moraine (Drift) do not complement one another .

Previous workers have recognized this situation but have
not correlated rock stratigraphy with morphostratigraphy in

101

this area. Any reinterpretation of the glacial geomorphology
associated with the Bloomington Moraine (Drift) must account
for three separate and distinct rock-stratigraphic units
within a feature that has been mapped as one morphostratigraphic
unit and also account for an ice source region that will
explain its fabric. An analysis of the tepography of the
Bloomington Moraine (Drift) indicates that it is not
necessarily one morphostratigraphic unit. Instead, it may
represent a situation.where three morphostratigraphic units
of different age converge on one another. This is substantiated
by the existence of three distinct rock-stratigraphic units.

The data of this thesis and the topography said to be
associated with the present east-west trending LeRoy and
Shirley Moraines (Drifts) indicate that these units could
equally as well be explained by north-south trending moraines
which extend to join the Heyworth Moraine (Drift) and
portions of the Shelbyville Moraine (Drift) (see Figures 4
and 13, in pocket). By interpolating between sections of
land outlined by the 750 foot (225 meter) contour, two or
three north-south trending landform units take shape which
intersect the Bloomington Moraine (Drift) at nearly right
angles (see Figure 17).

This alternate interpretation of the morphostratigraphy
can account for variations in the rock stratigraphy of the
Bloomington Moraine (Drift) by assigning the western Tiskilwa

Till to an east-west trending moraine, the eastern Malden Till

102

 

 

r'*__7
MCLEAN

CHAMPAIGN-
BLOCMING TON

INTERLOBATE

    
 

IGIV

IOMILES

g 5 I0 KM.

 

Figure 17 An alternate interpretation of the
morphostratigraphy of Central Illinois

 

103

to a relatively younger unconformable moraine more closely
associated with the Eureka-Normal Unit which contains this
same rock stratigraphic till member,and the Shamrock Till to
a previously unrecognized north-south trending moraine named
in this paper the Randolph. These interpretations are supported
by the preferred long-axis orientation of pebbles within each
respective till and are consistent with topographic
expression. The suggested name Randolph for the westernmost
north-south trending unit (see Figure 17) is for the town of
the same name in McLean County, Illinois, which is near the
crest of the postulated moraine (see Figure 13, in pocket).

The rock-stratigraphic correlation of the Shamrock Till
with the tills of the Shirley Drift, which are defined as
part of the Delavan Till Member of the‘Wedron Formation
(Willman and Frye, 1970), has been suggested by H. D. Glass.7
Because the study area of this thesis was restricted to the
boundaries of the morainal units under consideration, this
suggested correlation of Shamrock Till and Delavan Till was
not confirmed. It is suggested for future investigation that
the tills of the LeRoy, Shirley, and Heyworth Drifts be studied
and.ana1yzed in an attempt to establish their relationship to
the Shamrock Till.

 

7H. D. Glass, Clay Mineralogist of the Illinois State

Geologic Survey, in oral communication suggested this
possible correlation.

104

Conclusions on the Glacial Geomorphology
of Central Illinois

The morphostratigraphy, rock stratigraphy, and pebble-
orientation data examined in this study suggest the following
glacial chronology for central Illinois: (1) An ice advance,
possibly even pre-Woodfordian from the north, deposited the
Tiskilwa Till as a surface till on the Bloomington.Moraine
(Drift) to the west of the city of Bloomington, and this same
till was deposited over a wide area because it is an extensive
subsurface unit in the remainder of the study area. (2) An
ice advance from the east or east-northeast overrode the
Tiskilwa Till and deposited the Shamrock Till of the Randolph
Moraine (Drift), with a north-south trending drift border.
And (3) an ice advance from the north-northeast contemporaneous
with an ice advance from the east-northeast deposited the
Malden Till of the Bloomington Moraine (Drift) and Snider Till
of the Champaign Moraine (Drift) respectively, forming an
interlobate moraine named in this study the Champaign-
Bloomington Interlobate Meraine (Drift) in the area of ice
contact. The ice marginal retreat of the glacier to the
north-northeast was marked by a slight readvance to form the

Eureka-Normal Moraine (Drift).

Suggestions for Future Investigations
In a number of places in this thesis where data were
limited or where there was doubt about findings and inter-
Pretations, recommendations were made for further investigation.

The following is a summary of the suggestions for future

105
investigation of the central Illinois region as indicated by
the results of this study. (1) Of primary importance for
further study is an analysis of the relationships between
topography, till-matrix composition, and till-fabric orienta-
tion to the south of the Bloomington Moraine (Drift) of this
study. An alternate interpretation of the morphostratigraphy
of this region has been proposed. Additional investigation
may provide evidence to support this preposed alternate inter-
pretation. (2) The high degree of correlation between the
morphostratigraphic unit termed the Eureka-Normal Moraine
(Drift) and the rock-stratigraphic unit called the Malden Till
Member has been established by this study. This relationship
also exists between the Champaign Morphostratigraphic Unit
and the Snider Till Member. However, some of the relationships
between morphostratigraphy and rock stratigraphy along the
Bloomington.Moraine (Drift) remain unclear. For example, the
lines of demarcation between till members are questionable
and there is a need for further investigations of the till and
till fabric of the Bloomington Moraine (Drift) to establish
clearly the boundaries of the rock-stratigraphic units.
And (3) future studies of interlobate moraines might well
include an analysis of the till fabric in order to confirm
or reject the hypothesis of this thesis that the long axis
of pebbles embedded in the till of these landforms tends to

Prefer a parallel alignment to the associated ice-contact zone.

LIST OF REFERENCES

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108

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APPENDIX

Explanation of Data in the Appendix

Depth of Analysis -

Type of EXposure -

Topography -
TILL PEBBLE DATA:

Mmmmm-

Shape -

Strike -

Dip -

Misc 0 -

In feet below the crest of the
exposure

See Figure 8

See Figure 10

Longest dimensibn first, shortest
dimension last; all dimensions in
millimeters

(See Figure 12)

l. Tabular-elongate

2. Tabular

3. RhombOhedroid

4. Rhombdhedroid-elongate

5. Wedge-form-rounded

6. Wedge-form-elongate

7. Wedge-form-angular, subangular
8. Ovoid

9. Ovoid-elongate

Orientation of the pebble's long axis

Angle and direction of the pebble's
dip

S - pebble shows glacial striations

W - pebble was deeply weathered

LAV - long axis was vertical, there-
fore strike data is for
second longest axis

TILL MATRIX COMPOSITION DATA:

Grain-Size Distribution -

Carbonates -

sand 0062-200 m.
Silt 0004-0062 m.
Clay less than .004 mm.

? the existence is questionable
- none exists

111

112

Analysis Site Number __B_l___ Morphostratigraphic Unit Bloomington
Location NE NE NE Sec. 25, T.33N., R.3E. Quadrangle LeRoy
Elevation _8_6_C_J_'___ Depth of Analysis __L Type of Exposure Roadcut (old)
Topography C and D lepes on proximal side of moraine

Dimensions Li thol

z '0 Omite

r)

 

 

Fun—[Ecru emposfcronwca: Color Yellow tan Munscm Son Color No. 2.5Y 51¢

 

 

 

 

 

 

 

 

 

 

 

 

 

Clay Mineral Composition
’Crain-Size Distributlon xpandable ’Chlorite Carbonates’Cts;7Sec
SEE 1 Silt LClay Clay Illite] plus GlcTteTDolomite
22 L 40 L38 Minerals Kaolinite if I 70
6 BI l 13

 

 

 

 

 

 

Figure 18 Data for analysis site Bl

 

113

Analysis Site Number 32 Morphostratigraphic Unit Mimtom
Location NE NE SE Sec. 28#T.23N, R.3EJ. Quadrangle LeRy

 

Elevation 820' Depth of Analysis 8' Type of Exposure Roadcut (01d)

Topography D and E slopes near top center of moraine

 

a:

Dimensions Strike Li
lb 1 NEON Dolom to

(I
1
l .1 C
om te
RIO'-t
t
:0 Cr. C
below to
I FL‘
U0 Om
DO 0m CO
H. .1 t
most
it

lbmite

' 167nm
05177.1: ' '
CF13 anfarTC-e'- .-
Om
Li'nTc's F5717?
lémltC-——_-
- 57.115; LOT—fen-—
U- meETafie
_13nTE-§

.171] Ee

 

 

‘mix Canpoeition Data: Color Yellow canmnseu Soil Color No. 2.5Y 51¢

 

 

 

 

 

 

 

 

 

 

 

Clay_Mineral Composition
Grain-Size Distribution ’Eipandable Chlorite Carbonates Ctsg73ec
Sand I Silt 1 Clay Clay Illite plus Calcite:[¥bolomite
24 | 40 41 36 Minerals Kaolinite 11 41 ‘71
T 76 15

 

 

 

 

 

 

 

 

Figure 19 Data for analysis site B2

114

Malysis Site umber BB Morphostratigraphic Unit Bloomington
Location SE NE 58 Sec. 21, T.23N.L R.2E. Quadrangle LeRoy

 

Elevation 850' Depth of Analysis 25' Type of Exposure Roadcut (new)
Topography C and D slopes on distal side of moraine

e a:

Dimens ions
1 2 Dol omi re

,0!
30 om
‘0 Cm
ICI‘C
me e
0h 0
Inc". one
.: H U

' Ft
o It's
' 1c
__ -e .
Tomi tc

"parents"
OWE—e
5 one
DET— e
e

te

me 3 C one
e
om
e

 

tr x anpos on ta: 0 or ray rown Munse o 0 or o. .

 

 

 

 

 

 

 

 

 

 

 

 

Flay Mineral Composition
I CraTn-Size Distrifiltion Expandable CIIIoritc Carbonates Cts. Sea
:Sand 1 Silt I Clay Clay Illite plus Calcite Lbolomite
L '18 I 3" I_ 38 Minerals Kaolinite If I If

6 71 23

 

 

 

 

 

 

 

 

Figure 20 Data for analysis site B3

115

Mysis Site umber __Bfi__ Morphostratigraphic Unit Bloomington
Mfim SE SE SW Sec. 25, T.23N., R.25. Quadrangle LeRoy
Elevation 332; Depth of Analysis _?£'__'!ype of Exposure BOP?“ F13
Topography B, C, and D slopes on distal side of moraine

a:

Dimensions Strike Di Li thol
l 24 20 h SSE Dolomite

l ( ‘

arses_.a
LimQSLone_____
' e
“329'“.
10mite
558 Jolomitc
' omlte
ts.

1
nos one

mCS one
Om e

oml
F

 

Dd DFO

 

'mtrix CEstidon Data: Color Violet Munsell Soil Color No. 7.5? WIT

 

 

 

 

 

 

 

 

 

 

Fla Mineral Com sition
Grain-Si'zeTistribution ‘ ExpandaEle mOfltC CarFonai‘es Cts .jSec
Sand I Silt I Cla Clay Tllite plus Calcite LDolomite
29 I 38 L 35 Minerals Kaolinite 2.6 I 3,
S 71 '14

 

 

 

 

 

 

 

 

 

Figure 21 Data for analysis site B4

 

116

Analysis Site Number _§§___ Morphostratigraphic Unit Bloomington
Location NE NE NW Sec. 24, T.24N., R.MN. Quadrangle Danvers
Elevation _§ZQ:_ Depth of Analysis __2:___Type of Exposure Roadcut (new)
Topography B and C slopes near tap center of moraine 9

a:

Dimensions Strike

J

mes one
mastone
mcstone

 

 

"En—Piufi Composftion Data: Color Peach Munsell Soil Colormo.

 

 

 

 

 

 

 

 

 

 

 

Clay_Mineral Composition
Grain-Siie’Distribufion ‘Expandable ’Chlorite Canonates’Cfsg7SEC
Sand #1 Silt I" Clay_7 Clay Illite plus Calcite [:DOIEMIte
27 l 37 I: 36 Minerals Kaolinite 24 I 33
14 72 14’

 

 

 

 

 

 

 

 

Figure 22 Data for analysis site BS

117

Analysis Site Number 86 Morphostratigraphic Unit Bloomington

Location NE SH SH Sec.20, T.23N., R.68. Quadrangje Arrowsmith

 

Elevation 830' Depth of Analysis 5' Type of Exposure Pipeline Trench

Topography C and D slopes on proximal side of moraine

 

Dimensions Strike Lithol
Nbbw S ltstone
I . 1
N4‘ I 1rrz to
N MC 3 Cstone
0d I I r
{JD-(Iv! ‘ (:ran to

7‘ Dol

. 1t t
~- L)

“1“ "
“ In
'30
gm

( .

41993209
119.1. em“ to
t

1191.
Qbil§l._._____.
irons
-- -Ivimlilr" 'grls__._.
LC.C_511_§¢_._---
"01 9mm-

(

’91 mite

 

 

WEE-r1? Fmpoartloflsaca: Color Yellow tan Munsell Soil toIor No. 2.5Y 514

 

 

 

 

 

 

 

 

 

 

 

 

Clay Mineral Cempogition
Grain-Size Distribution EXpandable Chlorite -arFBhatcsiCtngSoc
Sand :1 Silt 1 Clay Clay Illite plus Calcite 1 Dolomite
24 I 35 '1 4l‘ Minerals Kaolinite ? ] 21
S 78 17

 

 

 

 

 

 

 

 

Figure 23 Data for analysis site B6

118

Analysis Site Number §§___ Morphostratigraphic Unit Bloomington .
Location guts: sw Sec. 27, 122er1 11.43. Quadrangle Arrwsnotn
Elevation __890_'__ Depth of Analysis __L Type of Exposure Roadcut (new)
Topography C and D slopes near tOp center of moraine

Dimensions Strike Lithol
l 9 7 N 3‘3 2 ho] omi

”LIN
J .

51):

F." r-

...1531 ___[3."‘S~11L
75.2.... ‘ :3. 13......
251_?_I~_l_ Li."‘.°£'l

it: unwise.--

u...

1.538. _--D9_lqn.i£c___

3’ -‘ JranseiioritL.

s.) (
-.S_. lloloni .tp.
D_9_1 om itc-

03.1.5.0-

r_l‘)0.l_0_mj_§_¢__.

0.0.1 911.99 __

 

00.1.0113?“
itc

:Qlomlts._ l

 

 

Maia: Compositionizata: Color Yellow can Munsell Soil Color No. 2 5X SL4

 

 

 

 

 

 

 

 

 

 

 

 

Clfl Mineral Composition
Crain-Sizcjlistribution xponiable "GU-onto ‘ -arbonatcs CESVSc-c
5.3an Silt I Clay Clay Illite plus. Calcite FIolomite
20 1 Al | 57 Minerals Kaolinite 3 j 33
5 81 14

 

 

 

 

 

 

 

Figure 24 Data for analysis site B9

 

 

119

halysis Site umber 312 Morphostratigraphic Unit Bloomington

Location WScc. 33. 1.234.; mss. Quadrangle Arrowsmith
Elevation 880' Depth of Analysis 7' Type of Exposure RoadCUC (01d)

 

topography B and C slepes near top center of moraine

e a :
Di [.1 thol

Dimens ions
J on» Do] omi to

88 51

alL .. _
Mlmitc,_,_
-.°hale --,
_-A_ Qvurtum—_--
... finale... _- .
LimestonL... _. ._
_.l'olomite _ .. _.__.e -
.llolomitc.-. ._. --a-_hL-
Juanita .- --_ _--_.- -.._

-—. no."

”Biotin __..°‘ _- - ___o. ._

__ DolonitLul:

 

 

Color Ye1low fan Munsell SoiTColor No. twin

 

 

 

 

 

 

 

'Wtrix ComposTtion Data:
‘ Clay HTnera] covmositTon ‘1
| Grain-Size Distribution Expandable ThToritc arbonatcs Cts.7§ec
[_Sand 1 Silt L Cla Clay Illite plus ' 7.1 m4 Dolomite
| 15 L 36 | 48 Minerals Kaolmte 8 j .141

' 5 1? EU

 

 

 

 

 

 

 

 

 

Figure 25 Data for analysis site 812

 

 

Analysis Site Number 31} Morphostratigraphic Unit

120

Location M NW NE Sec.l4, T.23N., RJB.

Bloomington

Quadrangle HCLCG"

 

Elevation. 790' Depth of Analysis 3'

Topography' C and D slopes on distal side of moraine

Dimensions

ZQN_

2

‘1

‘

Type of Exposure Roadcut (Old)

Lithol
one

Cherq__

32.11993. __

1' mpg;
.Cglts.op.___c
’ "tel." tout: ..

0

“Shall; . __
"j It; tone

£18.

Sins.
e

l._____‘._. .-

9911.29— -

“‘ --—.-——

Ilolpmietc.._._ _ _

Cranimilneia.

\

lolpmi Ce '

—.

 

 

 

Till flatrix Composition Data:

Col or PchT!

Munsell Soil Color No. lUYK 3i“

 

Clay Hi neral Composj t ion

 

 

 

 

 

 

 

 

 

[#Qrain-Size Distribution Expandafile 1 or te ‘ -arbonates Cts.lsec
I Sana_[ Silt j Cla Clay Illite I plus came 1 Dolomite
I 20 ‘I 46 1 34 Minerals Kaolinite 6 I ‘32

17 67 1 16

 

 

 

 

 

Figure 26 Data for analysis site 813

 

 

121

Analysis Site Number __§l1_ Morphostratigraphic Unit Bloomington
Location NE NE NE Sec.5, T.23N,L_R.lE. Quadrangle McLean
Elevation _§221_ Depth of Analysis __ng__Type of Exposure Roadcut_ggld)
Topography B and C slopes on distal side of moraine

e :

Dimensions Li
mes one

1
1
Color to
m_cr. tene -
rtgitc
omi
e
lomite __
wgmite
rt
a e

0..-

te

to

te
om

re

re
mestone
te
mon to

c ' ' l e
‘ te
H
N] e

FTill Matrix Composition Data: Celor salmon Munsell 3011 COIO:‘K67‘7TSYR‘STF"‘

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Clay Mineral Composition
rain-SIZE Distribution Expandable ‘Cfilorite ’Carbonatns Cts.7Sbc
sand Af'Silt I‘ Clay Clay Illite plus Calcite 1 Dolomite
22_ l_, 53 1 35 Minerals Kaolinite 13 ;I 27
l6 67 17

 

 

 

 

 

 

 

 

Figure_27 Data for analysis site 814

122

Analysis Site lumber BlS Morphostratigraphic Unit Bloomington

 

 

Elevation 790' Depth of Analysis 7' Type of Exposure Roadcut (01d)
Topography C and D slapes on distal side of moraine

 

Lithol
omite

d0 0’71 e

MES one
CF

13a
)0 Om e

' e

CETE636_"

0m L0
0m [0

nonfafié
Iolofilfe
>o'bfiito
)6jrv1n'm‘
ibfiflyc
Ithflflg..
“u.rt:it:
Dolomitz"::
-iofifiT‘
Ewaeur
.legmjtc
Dolomite
mafia
magma “'

ltStSfie

omite..

—.

e
0

e
m?§£999-.-
ts tone
_.__£9Q2.
_lomite
guartzite
SN? Li te
I L‘ 1 __ ._...
Qfl Sha
; )Q

 

0

 

VEHII‘EEcrxx Composition Data: Cdlor Salmon ‘anséll 3011 Cdlor No. 7:5YR 573

 

 

 

 

 

 

 

 

 

 

 

Clay Mineral Com sition ‘
CraifilSiie Distribution Expandable Chlorite Carbonates Cisi7§e6
Sand” I Silt I’ Clay Clay Illite plus a cite ! bolonite'
425 4]? _32 ]§ 57 Minerals Aaolinite 15 _]’ 25
20 66 14

 

 

 

 

 

 

 

 

Figure 28 Data for analysis site 815

21213

Malysis Site Amber 9,; Morphostratigraphic Unit Champaign
mum W "E SW Sec.9, Te20Ne. Re78e ”bangle mmt

 

 

Elevation 730' Depth of Analysis 9' Type of Exposure Rude“ (“9“)
Topography B and C slopes on distal side of moraine
a:

Dimensions Lithol
go 3 L mestone
|‘., 'l
“o omsto
mostonc
0211 1:0

‘udDUrO
mhst
JC t

I om

)0 on -

Om L

rt
no
__ te
Dior te
U154_E
W ' _ gougmite
it ‘ Ugigmlte
' ghert

Z ' ‘ -L’oth.
£131.92. __....

wasw Chert
__N.’»(w[ ._ “‘"DolomlT‘e "’

u .-.

Dolozni te “"
Dolomite—m '
mar-“-
Qfiarfii
“—Cliert’ ’ " "
"Tbléhit‘ew' ‘ "
Dblanifiz‘" '
‘Qfiirtiite‘
e
.I‘W '
"E:""""e -m
'r't

 

 

‘mufi Composition Data: Color Green grayuunselr Soil Color We. .

 

 

 

 

 

 

 

 

 

 

Clay Mineral Composition
FIRTH-Size Distribution Expandable Uulofite aflionates Cts. .ec
Sand 1 $11: 1 Clay Clay Illite plus WEE-377$ a‘"
26 41 38 17 36 Minerals Kaolinite ll‘—_ 1 23'
5 79 ' IF

 

 

 

 

 

 

 

 

Figure 29 Data for analysis site Cl

124

Analysis Site Number __C__2____ Morphostratigraphic Unit Champaiqn

Location NE NH NW Sec. 26L¥T.21N., R.6£. Quadrangle Gibson City
Elevation ___7_9_t_)_'_ Depth of Analysis _l_5_'_ Type of EXmsug-g Railroadcut (old)
Topography B and C slopes near top center of moraine

Dimensions Strike Lithol

91.0.91; :0...

J.t>.b£L._____
mimics ..__.

L__._._
l

Shale__
Chcrt

foloml' to
L ’Pt
Limrii’t'e' '”

Cabbro

 

il’t‘sTo‘n‘e ' ’
flvl‘slfl‘t“ "“ "

nnma&"”—

fiés’t’o'ne' ’
wee-{Stone
1‘51 ml to
O Om t5
0 own—iii!
.ran to
Isa '—
rt
{Julie——
’ 353E};—

~.—-—

 

 

Till Matrfi ComposTtion Data: Color Gm“ . Munsell Soil Color No. 2251 5(2

 

 

 

 

 

 

 

 

 

 

 

_ Clay Mineral Compofition
train-Size Distribution . Expandable Chlorite Carbonates Cts.7Sec
an 1 t ay Clay Illite plus CalciteiDoloqute
L 18 L 5') L 43 Minerals Kaolinite 8 j 15
2 83 15

 

 

 

 

 

 

 

 

Figure 30 Data for analysis site C2

125

Analysis Site Huber C3 Morphostratigrafllic Unit Champaign
Location NW NE NW Sec.9, T.22N.2 R.GE. Quadrangle Arrowsmith

Elevation _§_§_’_O_L Depth of Analysis 5' Type of Exposure Roadcut (old)
Topography B and C slopes near top center of moraine

Dimensions Stri ke

ll!
”01
. most
to
lolom CC
mentonc
mestofie
mcstonc
.I‘J

L 1 e
Dolomite
____E1mest

-—

Dolomite
-___.uga.r:t:éi_§c
te

t
;l on“:
quart—Bit?
11219359..
Cherg
lom

, —.

e

meeee-
995913.
8 ltstonc
te
e

rt
t
J to w

”'HII‘HarrIx Compoaruofliaca: Color Eve Wnse ”m 0 or . 2.9! 514

_

 

 

 

 

 

 

 

Clay Mineral Composition
Grain-Size Distribution ‘ Expandable Chlorite arfibnates Cts. er
a t a ‘ Clay Illite plus a c te'l Below to1
1 Minerals Kaolinite - I 17
2 83 I3

 

 

 

 

 

 

 

 

 

 

 

 

Figure 31 Data for analysis site C3

126

Malysis Site Number __g_4___ Morphostratigraphic Unit Champaign
Location SW SW NW Sec.32, T.22?!” R458. Quadrangle Arrowsmith
Elevation fl Depth of Analysis i Wpe of Exposure Railroadcut (old)
Topography B and C slopes on distal edge of moraine

a:

Dimensions Strike ‘ Li thol
N ' " om te

t

nt

-031}
DQJ 0m_1'£_c
inescene

l
_._.._, Dolml L12..._._.. ._.__...

...£ra12___.l___- __.-_ll

9_
L i
Dol

T-—-———-
11‘ 21te
P
I mOS

15.!
~ Om
mcstonc
"- te
OS . nert
2 e

‘mtrix Composifion Data: Color Gray Munsell Soil ColDr No. 2.3 522

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

_ ClaLliinera—l Comma ition
Train-Size Distrifiution . Expandfllle Chlorite arDTanates Cts.7Sec
a t ay Clay Illite I plus CaleitLI Dolomite
L 18 j 40 L 42 Minerals Kaolinite 9 J 20
V 2 79 L 19

 

 

Figure 32 Data for analysis site C4

127

mlysis Site masher _g6___ Morphostratigraphic Unit Champaig
Location SE NE NW Sec.33, T.23N., 12.68. Quadrangle Arrowsmith
Elevation _8_g_(_)_'_ Depth of Analysis #— Type of Exposure Roadcut (old)
Topography B and C slepes on distal edge of moraine

e

Dimens ions Li thol
l to

”I [‘0
mes tone
'1 “ALP

FE...
t 29m}.
(mite

1191.99.32..__
(.’her_t___
’0. ”O'nl te
Elem L's..-
Jamie-.-
holomi to.
Crani
Ilql
impelong.
quartzi te
Sha c
Dolomite
Uq_on t
_1 " t

 

l

 

Till Etrix Canpomion Nata: Color Gray tan Munsell Soil Color No. 2.5Y SZd

 

 

 

 

 

 

 

 

Clay Mineral Composition
ra n- ze str out on xpandfile Gllorite Carbonates Ctstec
mm a a Clay Illite plus Cilcite fDolomi te
- ' Minerals Kaolinite 10 I 17
2 85 l}

 

 

 

 

 

 

 

 

Figure 33 Data for analysis site CG

Analysis Site umber
Location Ed w W See. 15.
Elevation 910'

El

Depth of Analysis

128

Morphostratigraphic Unit Eureka

T.23N11iR.SE. Quadrangle Arrowsmith

6' Type of Exposure Roadcut (old)

TOpography B and C slopes near top center of moraine

Dimensions

Dolomi

V.

(.

1.9m

LC.“
mite
oml'
9&9
403W- 0
35:34! --__L)_Qlom ltv
Oi_.__4pkmne-.
19$- _. Siltstqnc ..
.DQlomite --...
2&_. que___
om h).-— -
itc.__._-

\

 

 

"fill—Haul): CompositionTata: Color Munsell Soil Color Yo.
Ian..— me...

 

 

 

 

 

 

 

 

 

 

 

Clay-Mineral Composition
rain-SizeTistribution Expandable Chlorite Carbonates Cts. l
a t a ‘ Clay Illite plus Calcite I Dolfige‘
45 18 Minerals Kaolinite - j 15
5 79 16

 

 

 

 

 

Figure 34

Data for analysis site 81

 

' 129

Analysis Site umber E} Morphostratigraphic Unit Eureka

Location 33 m m “9,23, 222W“ 3.3. Quadrangle Danvers

Elevation 830' Depth of Analysis 5' Type of Exposure Roadcut (new)

 

‘ropography B and C slopes near top center of moraine
e a:

Dimensions Strike

e)
-—

Dglomitf
1.96919
ipcstone
‘? It; £1099 -.

)o_l_o:n_i_t

D91993£9.__
teams;
1'1. '-
regs
“w-,

10m
Doiomi

10m
“ha 0

19m

4

 

 

 

 

 

 

 

 

 

 

 

‘mtrix Couposition Data: Color Tan Human Soil Color To. 2.5:: 53
Clay—Hifieral composition kpk,
CFaifiLSize Distrifiutlon xpandable ‘Chlorite Carbonates CtsiZSbc
Sand I Silt I Clay Clay Illite plus Calcite 1 Dolomite
I '10 I 40 Minerals Kaolinite 7 I 1]
4 78 18

 

 

 

 

 

 

 

 

 

 

Figure 35 Data for analysis site 83

130

Analysis Site Number :4 Morphostratigraphic unit Eureka
Location SE SW SW Sec. 34, T.25N., R.15. Quadrangle Danvers

 

Elevation 840' Depth of Analysis 5' Type of Exposure RoadCUt (old)
Topography B and C slopes on distal edge of moraine
e a:

Dimensions Strike Li
L 5 2 N E nstonc
r
f ‘ ‘ ' J0 r
3’32
'0
( H 3‘!
Pin
"hr-N
‘ Izu‘S
., ‘ln
' ' ll an) ‘
Polomi n
2410'?! LP
' H'!‘
n.
“.Jltf
,SICIH
flfirfi
'1 rt
Cd 3
“ha 0
F.0rt
% u
‘olom C
‘ranjii-
Dolgqitn
Dolomite
'dEEEmC
“9.1991.”
Chg§g___

9mizn
(out.
Quilts
"91001.21.
' in
CF

—---.- -

 

 

 

 

 

 

 

 

 

 

'quI—flitriiitamposition Data: ’Color 'Tan Munsell $611 Color 30. 2.§? 573 m
_ Clay Hineral Composition
’Crain-Size Distribution xpandable ‘Cfilorlte Carbonates Cts.7Sec
a t a Clay Illite I plus Calente I FoIomite‘
Hinerals Kaolinite l: *1 :2
r 83 i 13

 

 

 

 

 

 

 

Figure 36 Data for analysis site 84

131

Analysis Site umber __§_§__ Horphostratigrawic Unit Eureka
_Location SE NW NW Sec.lOA T.23N;J R.6£. Quadrangle Arrowsmith
Elevation .9_0_9__'__ Depth of Analysis _5_1___ Type of Exposure Pipeline Trench
Topography 81 C, and D slopes near tqp_center of moraine

e

Dimens ions Strike Li thol
J n mcztono

J] ' w 'o omite
”NPR OH!)
‘4 v
Om 0
C l
um
um
uU om
”AC.
I! l!‘ 7. (‘
.2 mo
l IPLZ C‘
mun one
)0 om e
OHI Q
‘0 (mutt:
(foul-oncrmre
Onito
)0 on: tv
{7575-1-
L.£§£°5P
.3314". L _:
Dolomite
. mostono
' .1 C
Chert
\ l e
i ltstonc
icrt
Omite
c 1 C
1 C
)aom 0
33.1? ’.’._ 'C‘
LJTfiFSrTEBEB“ ”TIM?“
(MLIFL15 Le '-“_—~_"
vdTBm n
rSTBEEto ’—‘“
L5 one
JO 0
l P
.! l C
. ‘ . A om e
't’ 507 ulJ c

- --.. c..-

I"
-l
.0

 

JR N . \NL L ~

 

‘mcrix Composition Data: Color Tan Munsell SoiI Color No. 2.5? 514

 

ClayffiinerallCom sitibn
ra n- ze nstr ut on ‘ Expandable "Chlorite arbonates fin-”15?:
a t L a} Clay Illite plus fllciLe 1 Dolomite

I_ 28 I 38 I 34 Minerals Kaolinite 8 _L I?

3 80 17

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Figure 37 Data for analysis site 85

132

Analysis Site Number _§§___ Morphostratigraphic Unit Eureka

Location NC cw SW Sec. 35;;T.24N,, R.6E. Quadrangle Gibson City
Elevation __§§2L Depth of Analysis __§:__ Type of Exposure Pipeline TPODCh
Topography B and C slopes near top center of moraine

a:
Lithol

CC

Dimensions
u

, l
l

(21.12.—

u__.__..
-____Lolumilu_._.
_v__”annlLu__--.--
.__ .Shalc.__._..

L.“ '3:- : " use.

I Igpitc

‘lint

aha 1.9— -

'Cihbro

061’ flit; _

t»_£§tone

lomite

stone

 

 

 

 

 

 

 

 

 

 

 

 

mgmte
J i o
(Ira tc
Till Hatrii’Camposition Data: Cdlor Tan HUnseIl Soil Color No. 2.5V 514
Clay_fiineraT’Com sition
raifiLSIze DistriButibn ‘ xpandable Chlorite arfionatcs’Ctsgjsec
a t ~- ay Clay Illite plus Cflcite 1 Do] oufito
24 4]_ 39 I 3] Minerals Kaolinite - p]: 15
3 81 16

 

 

 

 

 

 

 

 

Figure 38 Data for analysis site ES

133

Analysis Site Masher _E_ZZ__ Morphostratigrawic Unit Eureka
Location sw SE sw Sec. 244.2%” rues. qua-“91. Sibley
Elevation gl_O_'_ Depth of Analysis ____6__'_ Type of Exposure Pipeline Trench
‘I'Opography 8: C1 and D lepes on proximal side of moraine

e a:

Dimensions Strike Li thol
' I .1 I

P

(
lelnm to
I :I ‘r‘
‘; (atom?
I 't'
I ' - 1'
[10!0m t
(nu t
("71
j'TICI}
‘0 (ml
LCLLoglw‘
.l:“'.'SLOnC
291.0311 ~‘
on»
Dolomite
llqlomi
)o‘

119.1 emits. ._.. -
imestqno
‘QJ_0'_0.1'.§1__--,_
-DOIQWLLCC--
.Li ‘YECL'FQNQ-..
“new
.L‘hcrlm
Jilin“
1:110.
‘thl:
Ctr-r

—-

--“-—

 

 

 

 

 

 

 

 

 

 

 

 

 

'01..0_mi.t.g__
l .l
l
‘ l.-L§L______..
50 2?
‘mtrix Composftion Data: Color Tan Munsell Soil Color No. 2,5x 5‘4
ClaLHineral Composition
rafii-Size Distribution xpandab e mloritc arFonates Cts.fSec
Sand 1 Silt I Clay Clay Illite plus Cflcitel Dolomite
28 L 38 I 54 Minerals Kaolinite J J 9
4 81 L 45

 

 

 

 

 

 

 

Figure 39 Data for analysis site B7

134

Analysis Site umber _E_8__ Morphostratigraphic Unit Eureka
Location PM NW NW Sec. 3kT.23N.L R.38. Quadrangle LeRoy
Elevation _§_4_g'_ Depth of Analysis _5;_ Wpe of Exposure Roadcut (01d)
Topography B and C slopes on distal side of moraine

e ta:

Dimensions Lith01
1 ) [‘0 an LC
(1?!” L.
‘lSl t
)0 CmIM'
.‘. h! C I. ’OI‘US
'n or". L1:
mtnm KO
.imvntonv
(‘nvrt
to OH: [‘0
‘ “PM.
’0 011 LC
( PC
' ~rL
(' xert
ix) 0m "
.‘L |TT6
on”; (C
[stone
rt
'0 Om U“
112.01.11_LO
Shale

‘0 511758
f alt:-
__.n;:za§s_cooé:‘“" “
-Coloniks
‘eflq_.
style __A__
_MLS£QK___,
.2mony
“tm_u.-
'9L9mi§°_l
.lhwfiwm.
Ureyxmsm
JEEP

-—-—_.

I: 1.1“: {Cl-n 9

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

sues ._
m0
fiha
mo:
mg
ha]
1
1.1.413”
{Eelo'nLts
"19113
70w tst
Imtrix Composftion Data—Color Tan Munsell Soil Color No. 2.5Y 514
ClaJLMTneral Tom rosinon
rain-Size Distribution xpandable Chlorite arbonatesTtslSec
Sand ] Silt I Clay Clay Illite ' plus Calcitel Polo-nits
13 I 45 I 2; Minerals Kaolinite 6 j 21
3 81 in

 

 

 

 

 

 

 

 

Figure 40 Data for analysis site EB

135

Analysis Site umber 59 Morphostratigraphic Unit EugbL

Location up w m sec, go. 3.245.. 12.22; Quadrangle ml
Elevation 840' Depth of Analysis 5' Wpe of Exposure Roadcut Lnew)

 

 

Topography C and D slopes near top center of moraine
e a:

Dimensions
28

Uol’ to
l

[HalfjnI t

Dolom t

r
3Q10mitc
119
QQiQfllLC
I. I Inca; tone
[Riggs tn
‘fI‘n‘I‘C
66 om to
“9”?” Le
pol t
.Imrst
._ Dolor-Ilse.
P91911129
fioffifiile
Chcrt_
-.£191_°'_“_i£e.
1391951190
___L_i.mg_:_s tone _ __
Delgmiss -
_uartzite’m__
Iroiomite__
10mite
mestBfiE-
( ert
Iolomite
mestone
te
Jmestone
til I. C
)Y‘L
Tméztbnc
U25 (MU
Riga t
_Dolomite
___ 16:73:
Sandstone

-_—

 

 

n—v-

 

 

‘Wrix Composftion Eta: Color Tm unse So to or o. 2.5Y 37?

Im Tiomposftion

Grain-Size Distriiution Expandable Chlorite arbonates Ctsgzgic
Safid' I Silt’iI’ Clay Clay Illite plus Calcite I Dolomite
22 I 40 I? 38 Minerals Kaolinite 11 I :7

4 82 14

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Figure 41 Data for analysis site 39

136

Analysis Site umber E10 Morphostratigraphic Unit Eureka
Location NE SE SE Sec. 3, T.2SN., R.1w. Quadrangle Danvers
Elevation 770' Depth of Analysis 6' Type of Exposure Roadcut (new)

Topography C, DLand E slepes on distal side of moraine

 

Dimensions Li thol
? H01 Om‘i CC

( .

LL
1213 t
imvs
log; to
“.519- ' -UO
".732 ’ ‘ l9:
)1 l C O I_.:'ur.gs_t

( e

m: 29m: Chg-rt __
.‘ 5E2 Dolomite

205 ' Regg- .1 s
Q' J, gangs”
9“ £3.1st
holomi

ha

 

 

‘FflTTHatrix Composfiion Eita: Color Buff tan Munsell Soil Color Fe. 2.3? 51-1

 

_ Clfli ne ral Com mos iti on

_Grain-Size Diiwibution ExpandalIle Chlorite Carfionates Cts .ZSec
mm a ‘ Clay Illite plus ‘ Calm-$4 0 am e
_ . ' . Minerals Kaolinite '3 T 15

S 84 ll

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Figure 42 Data for analysis site E10

137

Analysis Site Huber Ell Morphostratigraphic Unit Eureka

 

Location 310 NE SE Sec. 34, T.26N., R.1w. Quadrangle Danvers

 

Elevation 700' Depth of Analysis 6' Wpe of Exposure Roadcut (new)

 

Tooography C, DL and E leJeS on proximal side of moraine
e a:

Dimensions Strike Lithol
J I) 7 S ‘ mm: [‘1 I'm:
'.(
’ LOI
‘ ’ - L 0:31 I C‘
' ' -!IZ(‘.'- on
firm" IP
’. LI IQ
h I mi
3:1".
. I.I-'.C
2 i'UEI 1‘0
,IIL.“ LU ‘
TI: fIl lL'
Iotn‘ Le
31-:':“~:E9_“£
I.l|_:}t.‘: COW:
.' H I_I'_
.9unyr
”0102150
were;
'91 9nd t"
"2' 99.1.11; ___...
‘__'~_-; 33);;‘34—01‘4 ‘0
Limestone
"I foII'oIn: to
-18.}1Mi—I'5.’
Illiii‘ilt
L TPEL'QUG
_polgmite
hol<;‘tc
Eii'LE_--_. _
Dolomite
HICTJO

_1.(7ni te ‘
111'] {STONES
__sthg’Z’ ”"
DO] Oflll LP
I‘D] (En-1' Lo
(TI—C}!
{VIII-v.2 Lone
; trmy£“““-
If)’ N I" (.17th
lb ‘ 3. TII C
or. " ;. : ~._Io
(M .. Itolom te
/LM 1» L'uIITtZILe
r’ MM '. i k ICI‘C

Whiz Camposition Data: Color Tan Munsell Soil Color No. 2.5? 3' 73 1

_ Clay Mineral Tongsi ion
l Grain-Size Distribution [Ypandflle I Chlorite arbonates CtsJSec
Illite

 

 

 

 

 

 

 

 

| Sand I Silt L Clo Clay plus Calcite IDolomite
I 16 I 55 I_ 29 Minerals Kaolinite 10 I 2o
‘ 5 GT L 13

 

 

 

 

 

 

 

 

 

 

 

 

 

Figure 43 Data for analysis site 811

138

Analysis Site Number N1 Morphostratigraphic Unit Normal
Location nw 35 NW Sec. lBLIT.25N.17R.68. Quadrangle _Arrggsmith
Elevation 830' Depth of Analysis 5' Type of Exposure Roadcut gold)
Topography B and C slopes on distal edge of moraine

e ta:

Dimensions Strike
1 {Il()€

I hr: I‘
HHIr mite
Ir T‘I t'
T:!("' 3_
39
V o t
(' :-
QJJCL31££_.__
1:4):
QI'I'
n:

 

 

kisb£_9£ye§
Dolomite

Sasalt

giltstone
orifiiic"'“““‘“""
3 lie
Eonite

“531C
.inustone
Qdarfzite
'itvt‘f-.‘—
DDSHTC
Dolomite
SolInEiE7r"“'”
fimvstofig-
xifiinite
I36 RBI-.11 to

7m ; {TE—EDEN

I; ' Isalt-_
‘ L

..

 

 

 

IFTillrflatrix Composition Data: color Tan Munsell Soil’COlor No. 2;SY S74

 

Clay Mineral’Com sitibn

Grain-Sizeibistribution xpandible Chlorite ar onates Cts£7Src
'Sand' I Silt fI_ Clay Clay Illite plus ‘ Salonte I Dolomite
l9 I_748 I 55 Minerals Kaolinite 6 I 15

6 78 16

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Figure 44 Data for analysis site N1

139

Analysis Site masher N2 Morphostratigraphic Unit Normal

 

Location SW NE NE Sec. 14, T.24N., R.1E. Quadrangle Danvers
Elevation 800' Depth of Analysis 10' Type of Exposure Roadcut (new)

Topography B and C slgxes on distal edge of moraine

Dimensions Strike
NUUN

an

Ami

ln'ni t

i -
"J' Qlfl

Urlgmilc

' O-

I _gte
_CILn‘ t
{£99330
om;
f“ g-(.
mystone

131991;
”iantone -
Limestone _____ _
3301 mi L_c_'_~______
ngomitg___
IIP’IPH '_ _
“.01 W11 t9--
' 015.159.
.1 playmate. _ _. ._ - -
1101991 §c__.____.._ _
1e1m09t909_
Unison...
“51°.ét9r13" __ ..
£‘ht‘.t.t1..l_____'olomite I-
(_‘hvr‘t_

 

 

 

 

 

 

 

 

 

 

 

 

21.15259"?
"0107911
Clem
I 91‘
s l e
. .10er
‘Uzl 21
b e
t-I‘dn
a. 0
11m narrTx Compositionbaca: Toior Tan Munsell soil ColorTo. 2.5xw 5/4
_ Clay Mineral Cbmposition
| Grain—Size Distribution xpandable “Chlorite - arbonates Pia/Sec;J
[f Sand :I Silt I Clay Clay Illite plus ‘ a ClLQ ‘o unite
[I 17 I 4] I 4? Minerals Kaolinite ll’ _j IE
3 83 14

 

 

 

 

 

 

a

 

 

Figure 45 Data for analysis site N2

140

Analysis Site umber _y_3___ Morphostratigraphic Unit Normal
Location NE SE SE Sec.4§, T.23N,1 R.4E. Quadrangle LeRoy_
Elevation 319; Depth of Analysis _6_'_ iype of Exposure Roadcut (01d)
Topography B and C slopes on distal edge of moraine

e

Dimensions Strike Lithol
' mes tone
(.‘.||
Inv.". tone
n JJC
OIOLI C
. mottone
. .f‘I‘I'II‘ItJCDIIEB
.I‘Q I‘m U‘.
I.('-:-'~.-()Y‘.L‘
‘ol’ImI—Wn
no UMII"
. nu}. tone
l OI.O_I_II int—C
mentone
lie
0.1.
(AH
U
ts L; _,
mestonc
Ug_9mlt
hob _ t
‘9199i§e_..
41010311.:
-IQOsq
U‘JOI; tens. _...-
Liwvgi9hv
.IOlOmi
___Ifolmnige” _
"0,I0_-'ni_t._<=_.-_-
Silrstone

(ELIH‘O- ___"
___90Jm.=i._tc.- __
51059099.- ,

aims-39m __..
POWELLC; '
_b_mostone ____
_ _ Fir-{eqiigitg ..I
5115329--
“he 19—
imestone
mestonc
lie-“3133..
Amiga-
"t

 

I)

 

 

'mtrix Composition Dita: Color Gray Tan mnsell Soil Color No. IUYR 512

 

 

 

 

 

 

 

 

 

 

7 Clayjfiineral Composifion
r'Crain-Siie Distribution Expandible ’Chloritc ‘Chrfionates Cts./Sec
[f Sand;;I Silt I ’Clayy Clay Illite plus Calcite‘IfDOlomits
F 12 1 :55 L30 Minerals Kaolinite 23 I 27

7 81 f 12 I

 

 

 

 

 

 

 

Figure 46 Data for analysis site N3

. 141

Analysis Site umber N4 Morphostratigraphic Unit Normal
Location NE NW NW Sec. 1, T.23N., R.2E. Quadrangle LeRoy

 

Elevation 860' Depth of Analysis 5' Type of Exposure Roadcut (new)
Topography B and C slapes on distal side of moraine

Dimensions Stri ke
NUUH

gird

l}(

 

lscstone
«mute .-_,
. .1_ni_tc
<uuq__
exits
r£..

'-

 

 

U}? __ __. _
L01 oral £13

1' was}.
L321 9102' E9
21.” 1339.-

imcgfi

ignite.

)9;

 

ni
1'

IMP}; L

 

 

 

 

 

 

 

 

 

 

 

 

 

 

0. ”Wit _

vmi

om
Tin—Eta: Composition fita: Color Tan Hunself boil Color No. 2.3? Sid
7 Clifiincral Composition
I Grarn-S‘ize Distribution xpandable Fluorite Carbonalcs figs.§::nH
| Sand f Silt I Clay Clay Illite plus ‘ a cue 17,0 on to
I 20 I 46 I 34 Minerals Kaolinite 10 J 29

4 83 1 13

 

 

 

 

 

 

Figure 47 Data for analysis site N4

142

Malysis Site umber _a_1_)_s__ Morphostratigraphic Unit Bloomington
Within 5!: SE SE Sec. 22LT.23N.4R.68. Quadrangle Gibson City
Elevation 359; Depth of Analysis __§_'___ ‘lype of Exposure Roadcut (01d)
topography B, CJ and n slopes on interlobate moraine

'9 e a:

Dimens 1 ans Li tho)
8 b 5 chm-t
Um
I. n mos tone
I I)
( mr‘
Il\»'
3111
‘I‘

"‘03 L

’17.C L
‘1?

_. {’6 1515.21 t2.

gas: 1.5:
__._...({U-U‘_t;§ 1.30...-
‘- 1.; Ilene ..
KUqHLZl
,l:olumi_l:c __. __
__ _l.i_nlcs_t_20_m_2___
. that.
_(‘hcrtm
- ”__1391 Quite
_Sh-Ilpa _ ..
I'm-92mm- _ -
1923993....
9;“.139_

omits_____

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

111??!“qu ComposTtion Data: Tolor Tan Tfimsa] Soil Color No. .9411. a £4
Cl.11Mineral Composition
min-Size Distribution Expandiblc Chlorite Carbonates Cfs. .mc
SanJTSiltj Clay Clay Illite I plus Falcfic 1 Dolomite
19 1 714 L 3‘! Minerals Kaolinite __I 21
3 L L 12

 

 

 

 

 

 

 

Figure 48 Data for analysis site BDS

143

Analysis Site Number BD7 Morphostratigraphic Unit Bloomington

Location SW NW NW Sec.24,_'r.23rl.l R.GE. Quadrangle Gibson City

Elevation 820' Depth of Analysis 5' Type of Exposure Roadcut (01d)

 

Topography C and D 5109625 on interlobate moraine

0 Cd!

Lithol
Granite
”(“1
'Ti L '. mm
m t

f'

Dimensions

r-

". 1‘ ‘
wattage
303.9“: to
\

h. Ali..-

 

C

 

ll'ill Matrix Composition Data: Color Tan Munsell boil Color No. 2.§\7_§Z§ _

 

 

 

 

 

 

 

 

 

Clay Mineral Com wositi on ‘
Grain-Size Distribufibn Expandable Cbloritc ‘ 7F3?bonatn§’?ts.1§e€
an o t a‘ Clay Illite plus Fulci Lc'l—Tinbmifé‘
[:i 2? I 40 L__7$U Minerals Kaolinite I ‘1 In
3 85 l 2

 

 

 

 

 

 

 

 

Figure 49 Data for analysis site BD7

143

Analysis Site lumber'_jg§L_ Morphostratigraphic Unit Bloomington
Location sw Nw Nw Sec.2§1_:.23fl., R.68. Quadrangle Gibson City
Elevation _8i_0'_ Depth of Analysis __5'___ Type of Exposure Roadcut (old)
Topography C and D slgges on interlobate moraino

ta:

Dir-ens 1 ans Strike Li thol
N7Unl Crani te

‘7 '2 mm
Mn '

1:291;L;QD0_____
.‘QlQm
huln_-

__.L..." ‘ “ 2L ._.
_-_1291_°'F‘i
._Ch¢ _
90!;
.Iawmlerlc
rt

£11913;
Limestone —

 

(

 

Till Matrix Composition Data: folor "Tm Munsell soil Color Yo- 2.§~’_>Z§ - '

Clay Mineral C‘ommsition

 

 

1

 

 

 

 

 

 

Grain-Size Distribufion xpanciable Chlorite Wi'rbonates MmftTcTc‘
Sandj Silt L Clay Clay Illite] plus i'ulcz'tefifilbnifé‘
2? I 40 L 58 Minerals Kaolinite I ] I...
3 85 l .12

 

 

 

 

 

 

 

 

 

 

Figure 49 Data for analysis site BD7

 

144

Analysis Site Nu-ber ggg Morphostratigraphic Unit Bloomington

Location :3 5y NH Sec,8. T.23}!u R.7E. Quadrangle Gibson Pity

Elevation 800' Depth 0! Analysis 8' Type of Exposure Roadcut (old)

“WWW WWW nc

 

 

Dimensions Sha Strike Di Lithol
5' H Basalt

 

—-_-..

. 1 '
.3 51—-..

‘ Q1 mils..__
‘ v.12__ __

V

 

 

 

 

 

 

 

 

 

 

 

 

‘fi Matrix Composition Data: Color Tan Hansen Soil Color No. ?.SY 514
Clay Mineral Composition
Crafix-Cize Distribution Expandable Chlorite Coflonalos Cfs.7§ccl
and’#[ Silt iIi Clay Clay Illite plus Calcife I Dolomite
29 1 3b 417 55 Minerals Kaolinite 3 I lo
5 82 13

 

 

 

 

 

 

 

Figure 50 Data for analysis site BDB

 

145

Analysis Site Number BP7 Morphostratigraphic Unit Bloomington
Location SE NE NE Sec.20, T.23N., R.6E. Qnadranglg Arrowsmith

 

Elevation 930' Depth of Analysis 5' Type of Exposure Pipeline TI‘CDCh
Topography 8 and C slopes near edge of interlobate moraine

 

a:

Dimensions - Li thol
J S 5 bran to

S t: one
Eran e
320 On
:7 mr
HTS one
:0 on C
)0 09:: LC
)0 Om
JUJI‘LZ C
‘. '-.'. one
I Il'L’i’. L0
121 .ro
DO ( C
I‘LL-733510
finiall.
HO 0.“ C
30 (m. (‘
‘Ol (in te

r.':
an! e)

 

\ F

omite
101 e
.iltstonu

\li'AJL/b U

 

4
0m
"-_—Crahitc
Sim Sil't—stone
DolomiCe
'-—Qu7?F2ité'-‘-‘

-158W- 'Cieéfistohé-‘

- 5M4- _M'Quart'él'te“ .
__— Clfifitfifl- '
'—_'[Yfi33?ohcd'_.
"*wl%lsltc -“'

_ FFH‘Vimofitono

-'inorit§.."'. ”"
Eilffifafie'_
lolEIJtc
Folonltc
.fibfidfi'
“Tomlto' "
POTBEiTC_——_-~“
to 0m 0 '— ““-
holfifiifc
“losgtofié‘ - -.
Cfinle --_”-"'

 

 

 

Till Matrix Composifion Data: Colomllow tun Munsell Soil 7folor No. 2.51514

 

 

 

 

 

 

 

 

 

 

 

 

Clay Mineral Composition
Gain-Size Distribution Expandable Clilorite arFonates‘F‘tsJSec
Sand I Silt f Clay Clay Illite plus Calcite I l‘olomite
24 i 36 | 40 Minerals Kaolinite_4 7 I 17
j 83 3.2

 

 

 

 

 

 

 

 

Figure 51 Data for analysis site BP7

146

Analysis Site masher 8P8 Morphostratigraphic Unit Bloomington

Location SE SW sw Sec. 21. T.24N., R.7E.

Quadrangle Sibley

Elevation 810' Depth of Analysis 5' Type of Exposure Roadcut (Old)

Topography C and D slopes on interlobate moraine

Di mens i ons

Lithol
C ltstonc
LI
3c] C
( artz to
l to

('hvrt
Do] to
:20 (mute
fl l e
V tstone
I o
e
om to
)o L
me C

‘. ml
at; u)’e‘__:“""""
9.1.09.1}
: .1.le£c‘..__
(Milt- , -

( igtzi tg
__ "__pol 9311p?

---—

Cher;
imns tenc_
_J‘QJ Omit?“

_l 1.5.1.1 £1990.
onl_i_t__n___
__gdml e _ __ _. _._
lomj t9. ,,,,,,
_‘iuifl 241-93. .

o.»

mostone
Li mg_s gone -.-..

(

 

 

 

Till Matrix Canposition Data: Color—Yellow tan Munsell Soil Cfior No. 2.5Y S74

 

 

 

 

 

 

 

 

 

 

 

 

 

CIaLfiinerTf Commsition
Train-Size Distribution xpandable 'Cfilorite ‘ arbonates Elm/fies}
Sand 1 Silt I Clay Clay Illite I plus Calcite hi010lfit0
25 I 42 I_5T Minerals Kaolini te ll) I Fr
b 81—7 L 15

 

 

 

Figure 52 Data for analysis site 3P8

 

 

Analysis Site ”her new Morphostratigraphic Unit
Location NW N SW Sec. 14, T.23N., R.6E.

147

 

 

Elevation 8 70 '

Depth of Analysis

Topography B and C slopes on interlobate moraine

Dimensions

Strike

Bloomington
Quadrangle Gibson City

 

" Ty" of Exmsure Roadcut (Old)

Li thol
(ml 0

_..._;.'n.lle __l... H..- _
Jif'gfilEOIlg ___.

Chert

o”.-- _—

__..- .. LOLM'CE... _

o.--

Shale- -. -.
volgnlrs.--
:IhllC—m _
limestone. __
Rmeflq;___
Limesggnp
r52} te ..
__Lhegt. _.
"03.92133.”
Shalq____
'qu9;-_
.i - t
am;
,:
DOlOmltOm_
30 it
olomite
inwgmo

-.—-

Dolomite“

Sign} O _

I'M‘.S.£<1rlé_:
b “43.2
Chqflg- _-M-
“91.9811 :0... --_
: xolomi_tg_

 

 

 

Till Matrix CampositioniData: ’Color Yellow tan Munsell COil Celor No._—YT5Y 577‘":—l

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Clay Mineral Composition
Grain-Size Distiibution ‘xpandable Chlorite ‘ CarbonatesiClsi7§e&1
Sand L Sil t T Clam Clay Illite plus Cal CI to ij‘ol 0:13 to
22 III—40 II SB Minerals Kaolinite ? I Lb
7 78 15

 

 

 

 

Figure 53

Data for analysis

site BPlO

148

Analysis Site Huber BPll Morphostratigraphic Unit Bloomington
Quadrangle Cihson City

Location NW NE NW SOC. 12. T.25th H.6R.

Elevation 850' Depth of Ana

lysis 10' Type of Exposure Roadcut (old)

Topography C and D slopes high on interlobate moraine

e a:

Dimensions

Strike

N

NZUL

J

 

Lithol
1. tstone
‘ |
no om to
so: Ce
{ ICFL'
(.‘nC‘l‘C
L: rt
polan to
’J C 1‘?
C'D CC
\( om tn
1.“! ’ tone
rd 0
10m te
Hustone
“Olgqltc
A I
J alt
rust
vans
Polgmi
imn§s__
:plogite
lgn
imchggg
gplrtgite
"blYC
_ rt
__.vglomits-
Dolomite
Red Limes one

391.913: .
PQQEEL.
:rt
QEQEEL.
DOlOmlte.
s. le

Quiz-'- 35¢

to?

_ Sh“; "’
-2511 ,
Siltstone
GlElTE'”
“lale
. 55if5_"—-_—“ _-—‘”’——”

--._, — __-,._..._

 

 

 

‘Wrix Composition Data:

Color Yellow tan HunselT Soil Color No. KW 57‘?

 

Clayifiineral Composition

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Grain-Size Distribution ‘Eipandable Chlorite ‘ Chrbbnates Cts(7§r€
Sand II Silt I Clay Clay Illite plus Calcite l Dolonite
20 I 42 I 58 Minerals Kaolinite 12 1 ID

6 81 13

 

 

 

 

Figure 54 Data for analysis site BPll

 

149

Analysis Site lumber £32 Morphostratigraphic Unit Eureka
Quadrangle Danvers

Location NE 52 us Sec.3, T.2SN.L

Elevation 750' Depth of Analysis

Tmanflw

R.1W.

23' Type of Exposure Roadcut (new)

Strike
0w

? (stratigraphically lower till unit, top till see E10)

 

 

 

thol
Dolomit

 

l
Dolomite_____..
mutant—
- Shale____._
Limestcncu.__
_. limes tone—___
-_._.HQlQmitc_t
J‘ l:
.__“quairc-
" alt.
Iolomitnuu
Dolomite.
£130.11--- __
.Lkundss___.~.-
mlplni.te____-

I

..

 

 

 

 

 

 

 

 

 

Till Matrix Composition Data: Color Red brown Munsell $011 Color Nb. 2 318 SKA
Clangineral’Composition
rain-Size Distribution xpandable ‘Chlorite arbonates Ctsg7SEC
Sand I Silt I Cla Clay Illite plus ‘ Calcite lilfiflimdte
27 1_441 1 3? Minerals Kaolinite 422 1’ 2h_
14 70 15 ‘

 

 

 

 

 

 

 

 

 

 

Figure 55 Data for analysis site 882