stratigraphic framework and landsystem correlation for

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Stratigraphic Framework and Landsystem Correlation for Stratigraphic Framework and Landsystem Correlation for

Deposits of the Saginaw Lobe, Michigan, USA Deposits of the Saginaw Lobe, Michigan, USA

Ivan R. Guzman

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STRATIGRAPHIC FRAMEWORK AND LANDSYSTEM CORRELATION

FOR DEPOSITS OF THE SAGINAW LOBE,

MICHIGAN, USA

Ivan R. Guzman, M.S.

Western Michigan University, 2014

Since the time of the Last Glacial Maximum (LGM) the south-central portion

of the Lower Michigan Peninsula has been subject to several glacial advances and

retreats by the Saginaw lobe. As part of the U.S Geological Survey Great Lakes

Geological Mapping Coalition projects, several rotosonic borings were drilled

between 2006 and 2013 in Barry, Kalamazoo and Calhoun Counties. Gamma ray logs

and textural analyses were completed for each core. Five of these borings were

selected according to their diamicton (till) content and correlated using water well

logs and surficial geology maps. Glacial deposits such as diamicton serve as

evidence of glacial advance/retreat, and are usually present as nearly continuous

layers of sediments. Analysis of these layers affords the ability to accurately correlate

these types of sediments across an area. Three cores, BA-10-02 and BA-09-02, KA-

12-02 were drilled along the Kalamazoo moraine, each one containing 1 to 3

diamicton units separated by lacustrine sediments. The last two cores, CA-11-01 and

KA-13-01 were drilled on a drumlinized till plain; both contain 2 to 4 diamicton units

separated by outwash sediments. These diamicton units indicate the presence of at

least one major and two minor advances/retreats of the Saginaw Lobe.

STRATIGRAPHIC FRAMEWORK AND LANDSYSTEM CORRELATION

FOR DEPOSITS OF THE SAGINAW LOBE,

MICHIGAN, USA

by

Ivan R.Guzman

A thesis submitted to the Graduate College

in partial fulfillment of the requirements

for the degree of Master of Science

Geosciences

Western Michigan University

June 2014

Thesis Committee:

Alan E. Kehew, Ph.D., Advisor

Rama V. Krishnamurthy, Ph.D.

Upul B. Attanayake, Ph.D.

Copyright by

Ivan R. Guzman

2014

ii

ACKNOWLEDGMENTS

I would like to thank Dr. Alan Kehew for his guidance, advice and patience

during the realization of this project. I am grateful for the help of my committee

members, Dr. Rama Krishnamurthy for his continuous help and support in the early

stages of my project, and Dr. Upul B. Attanayake for collaborating with me and

offering me advice. I also offer my sincere appreciation to my country, the

Dominican Republic for providing me with a scholarship as well as the necessary

funding to live and study in the United States. I would also like to thank the WMU

Department of Geosciences, the WMU Graduate College, the W. David Kuenzie

Research Fund and the U.S Geological Survey Great Lakes Geological Mapping

Coalition from whom I received funding for this project.

I would like to express my gratitude to Stephanie Ewald, Abdou Mohammed,

Derrick Lingle, Sita Karki, Todd White and many others for their various

contributions to this project. I thank Racha El Kadiri for her support and

encouragement, which helped me to overcome many obstacles during my graduate

career. Lastly, I would like to thank my family for their unconditional support and

patience. They always believed in me and kept me motivated to stay on track and

reach my goals.

Ivan R. Guzman

iii

TABLE OF CONTENTS

ACKNOWLEDGMENTS ...................................................................................... ii

LIST OF TABLES .................................................................................................. vi

LIST OF FIGURES ................................................................................................ vii

CHAPTER

I. INTRODUCTION ...................................................................................... 1

Previous Investigations ........................................................................ 2

Site Description ................................................................................... 4

II. GEOLOGY ................................................................................................. 7

Bedrock Geology ................................................................................. 7

Wisconsin Glaciation in Michigan ...................................................... 11

Saginaw Lobe Landsystems ................................................................ 14

III. GEOCHRONOLOGY ................................................................................ 17

Glacial Geochronology in Michigan ................................................... 17

Radiocarbon Dating on Glacial Till: Main Concerns .......................... 18

IV. METHODS ................................................................................................. 20

Particle Size Analysis .......................................................................... 20

Atterberg Limits .................................................................................. 25

Bulk Organic Carbon Assay ................................................................ 29

Inorganic Carbon Assay ...................................................................... 31

Map and Cross Section Data ............................................................... 32

Table of Contents—Continued

iv

CHAPTER

V. RESULTS ................................................................................................... 34

Landsystem 3: North of the Thornapple Valley .................................. 34

BA-09-02 ..................................................................................... 34

Landsystem 2: South of the Thornapple and North of the

Kalamazoo Valleys .............................................................................. 38

BA-10-02 ...................................................................................... 38

KA-12-02 ...................................................................................... 42

Landsystem 1: South of the Kalamazoo Valley .................................. 45

CA-11-01 ...................................................................................... 46

KA-13-01 ...................................................................................... 49

Diamicton Clay Consistency ............................................................... 53

Cross Section A-A’ ............................................................................. 55

Radiocarbon and δ13

C Analyses .......................................................... 59

VI. DISCUSSION ............................................................................................. 63

Core Interpretations ............................................................................. 63

Landsystem Correlation across the Saginaw Lobe .............................. 70

VII. CONCLUSIONS......................................................................................... 75

APPENDICES

A. Particle Size Analysis Results .................................................................. 77

B. Atterberg Limits Results .......................................................................... 105

C. Bulk Organic Carbon Results .................................................................. 125

Table of Contents—Continued

v

D. δ13

C Results ............................................................................................. 127

BIBLIOGRAPHY ................................................................................................. 129

vi

LIST OF TABLES

1. Boreholes: Coordinates, Depths and Elevations ............................................ 6

2. Interpreted Water Well Lithology .................................................................. 33

3. Diamicton Clay Consistency Data Results .................................................... 54

4. Diamicton Bulk Organic Carbon Data ........................................................... 61

5. Diamicton Carbonates Data ........................................................................... 61

6. Carbon 14 Data Results ................................................................................. 62

vii

LIST OF FIGURES

1. Study area and borehole locations in southern Michigan. ............................. 5

2. Bedrock geology, south-central portion of the Lower Michigan

Peninsula. ....................................................................................................... 9

3. Interaction between the Saginaw, Huron-Erie, and Lake Michigan

Lobes .............................................................................................................. 13

4. Landsystems of the Saginaw Lobe, Southern Peninsula of Michigan ........... 16

5. Wentworth grain-size scale for sediments ..................................................... 24

6. Clay consistency and Particle size analysis tools .......................................... 28

7. Logplot Diagram of BA-09-02 showing lithology, gamma ray

signature, and grain size distribution ............................................................. 36

8. Matrix texture (<2.00 mm) of all samples in BA-09-02 ................................ 37

9. Logplot Diagram of BA-10-02 showing lithology, gamma ray


10. Matrix texture (<2.00 mm) of all samples in BA-10-02 ................................ 41

11. Logplot Diagram of KA-12-02 showing lithology, gamma ray


12. Matrix texture (<2.00 mm) of all samples in KA-12-02 ................................ 44

13. Logplot Diagram of CA-11-01 showing lithology, gamma ray


14. Matrix texture (<2.00 mm) of all samples in CA-11-01 ................................ 48

15. Logplot Diagram of KA-13-01 showing lithology, gamma ray


16. Matrix texture (<2.00 mm) of all samples in KA-13-01 ................................ 52

17. Location of cross section A-A’ ...................................................................... 56

List of Figures—Continued

viii

18. Cross Section A-A’. ....................................................................................... 58

19. Matrix texture (<2.00 mm) of diamicton samples in BA-09-02. ................... 64

20. Matrix texture (<2.00 mm) of diamicton samples in BA-10-02 .................... 65

21. Matrix texture (<2.00 mm) of diamicton samples in KA-12-02 .................... 66

22. Matrix texture (<2.00 mm) of diamicton samples in CA-11-01 .................... 68

23. Matrix texture (<2.00 mm) of diamicton samples in KA-13-01 .................... 69

24. Matrix texture (<2.00 mm) of diamicton samples from cores: BA-09-

02, BA-10-02, KA-12-02, CA-11-01 and KA-13-01 .................................... 71

25. Cross Section A-A’: Proposed Correlation of Sediments .............................. 72

1

CHAPTER I

INTRODUCTION

Since the time of the Last Glacial Maximum (LGM), sediments from three

lobes of the Laurentide Ice Sheet have dominated the Lower Peninsula of Michigan.

After the LGM, the first lobe to retreat was the Saginaw lobe, but not before

experiencing a series of small advances and retreats (Kehew et al, 2012a). Today,

only small portions of the surface landscape of the Saginaw Lobe has been mapped,

and very little is known about the characteristic of the region’s subsurface deposits as

well as how these deposits correlate with the advance and retreat of the ice. Recently,

studies have examined the subsurface deposits of the Saginaw Lobe, but only a few

borings have reached bedrock and fewer still have mapped the subsurface

stratigraphy of these glacial deposits. This study is intended to work out the

subsurface stratigraphy of the Saginaw Lobe. For that purpose, five rotosonic

boreholes were drilled in the counties of Barry, Kalamazoo and Calhoun, Michigan.

These borings were selected according to their thickness and stratigraphy.

The principal objective of this research is to identify and map major

stratigraphic units across the south-central portion of the Lower Peninsula of

Michigan related to glacial advances/retreats and investigate if these units can be

correlated through the area. A second objective of the study is to characterize the

glacial drift stratigraphy by interpretation and documentation of lithological units in

the Saginaw Lobe. Cores drilled along the Saginaw Lobe have shown diamicton a

2

few meters above the bedrock. This study will demonstrate if the diamicton units

correlate with each other and if the units are related to glacial advances/retreats.

Water well logs and a bedrock topographic map are used, as well as textural,

consistency and geochronology analysis to more clearly understand the glacial

deposition of the Saginaw Lobe.

Previous Investigations

The first studies to map the surficial deposits of the Saginaw Lobe, were

performed by Leverett and Taylor (1915). Based mostly on topographic analysis,

these studies describe Michigan surficial deposits by identifying and mapping various

glacial landforms, including the end moraines of the Saginaw Lobe, which they

associated with ice marginal positions. Martin (1955) compiled the first revised map

of the surficial geology of Pleistocene glacial deposits in Michigan. The map shows

the general distribution of glacial landforms across the southern Peninsula of

Michigan. Later Farrand and Bell (1982) published a revised map of the Quaternary

geology of southern Michigan that includes textural descriptions derived from the

previous soil surveys. Monaghan and Larson (1986) identified and correlated two

upper till units in south central Michigan, the Bedford and Fulton tills, using grain

size distribution and clay mineralogy analyses. Using only six 9-meter boreholes and

other surface samples, the authors traced the Bedford till from the Lansing Moraine to

the Kalamazoo Moraine and the Fulton till from the Lansing Moraine to the Tekonsha

Moraine. From this investigation they reach the conclusion that the Kalamazoo

3

Moraine of the Saginaw Lobe could be correlated with the Kalamazoo Moraine of the

Lake Michigan Lobe, and to the Powell Moraine of the Huron-Erie Lobe.

In the last fifteen years, new research has incorporated stratigraphy,

morphology, and clay mineral content of diamicton units into glacial studies (Taylor

et al., 1998; Fisher and Taylor, 1999; Kozlowski, 1999; Kehew et al., 1999;

Kozlowski et al., 2001; Fisher et al., 2003; Kozlowski et al., 2004; Kozlowski et al.

2005; Kehew et al 2012a). Woolever (2008) focused on the surface geology created

by subglacial meltwater of the Saginaw lobe. He concluded that several linear valleys

containing eskers in Barry County were tunnel valleys produced by meltwater erosion

at the base of the glacier. This finding helped to further understand the dynamic in

drainage systems of the ice sheet and how tunnel valley and eskers were formed.

Barnes (2010) analyzed till samples looking for systematic variation in the organic

matter content that could potentially explain the high iron concentration in

southwestern Michigan groundwater. He found that high organic carbon content was

most likely producing the higher iron concentration in the groundwater.

Recently Kehew et al (2012a) proposed a four landsystems approach to

classify the surface terrain of the Saginaw Lobe in Michigan according to the

sediment/landform relation in the lobe. This made it possible to interpret the glacial

dynamic and interactions between the ice and the substrate in the Saginaw Lobe.

Kehew et al (2012b) also described the role of subglacial meltwater flow systems in

the formation of tunnel valleys and concluded that subglacial water flow in tunnel

valleys played a crucial role on the drainage and stability of the ice sheets. Ewald

4

(2012) using data from six cores, reconstructed the depositional environment for the

glacial and lacustrine sediments present in Barry and Calhoun counties. She

concluded that several intervals within these borings were associated with a

proglacial or subglacial lake not previously identified in the Lower Peninsula of

Michigan.

Site Description

The area of study in this analysis is located in the south-central portion of the

Lower Peninsula of Michigan between the counties of Barry, Kalamazoo and

Calhoun (Figure 1). Between 2009 and 2013, five rotosonic boring were drilled in

several sites along these areas. The boring sites were selected to develop a

generalized stratigraphic framework and to determine the stratigraphy of tunnel

valleys in the study area. .

The first group consists of two boreholes drilled in Barry County; BA-09-02

drilled in 2009 and BA-10-02 drilled in 2010. The second group was drilled in

Calhoun County and consists of one borehole; CA-11-01 drilled in 2011. The third

group consists of two rotosonic boreholes drilled in Kalamazoo County; KA-12-02

was drilled on 2012 and KA-13-01 drilled in 2013. Most of the boreholes are located

within tunnel valleys or glacial uplands to aid us in better understanding the overall

drift stratigraphy in the area (Table 1).

5

Figure 1. Study area and borehole locations in southern Michigan. Borehole are

labeled and marked with red circles.

6

Table1

Boreholes: Coordinates, Depth and Elevations

Core ID Latitude Longitude Depth (m) Elevation (m)

BA-09-02 42.7285 -85.2053 63 247

BA-10-02 42.5532 -85.1886 85 292

CA-11-01 42.2823 -85.2424 55 305

KA-12-02 42.3622 -85.3361 81 286

KA-13-01 42.1313 -85.3255 49 293

7

CHAPTER II

GEOLOGY

Bedrock Geology

The glacial deposits across the Michigan Southern Peninsula are mainly

composed of material eroded from bedrock or previous sediment along the path of ice

movement from ice-sheet centers near Hudson Bay (Monaghan and Larson, 1986;

Dodson, 1993; Gardner, 1997; Flint 1999). Understanding the bedrock geology is

crucial towards gaining a fuller understanding of the stratigraphic settings of these

glacial sediments. The Michigan Basin is formed of sedimentary rock units of which

1% comes from Pennsylvanian age, 5% from Mississippian, 16% Devonian, 30%

Silurian, 21% Ordovician and 27% Cambrian (Cohee 1965; Dorr and Eschman 1970).

These sedimentary rocks can be grouped in a series of formations (Figure 2). The

bedrock formations are part of the Michigan Basin, which is an elliptical intracratonic

basin, located against the southern margin of the Canadian Shield (Gillespie et al.

2008).

Bedrock formations subcrop beneath the glacial deposits in a series of

irregular concentric rings (Figure 2). The ages of these formations range from

Cambrian at the margins of the basin to Pennsylvanian in the center, capped by a

small area of Jurassic rocks. The basin strata are mainly dominated by dolomite and

limestone, with a significant presence of siliciclastics (shale, sandstone and siltstones)

8

and evaporites (gypsum, halite) (Dorr and Eschman, 1970; Howell and Van der

Pluijm, 1999).

During the Pleistocene, bedrock topography played a crucial role in the

advance of the Laurentide Ice Sheet sub lobes by controlling their boundaries (Kehew

et al, 2012a; Ewald 2012). In the course of this time period, bedrock formations

across the Michigan basin were buried beneath thick unconsolidated glacial sediment

carried by the continental ice mass. Studies made by Dorr and Eschman, (1970) and

Harrell et al, (1991) have estimated that the thickness of these glacial deposits varies

in different locations ranging from 0 to more than 305 m (1000 ft).

The area of study is located in the southwestern part of the Southern Peninsula

of Michigan and includes the counties of Barry, Calhoun and Kalamazoo (Figure 2).

The uppermost bedrock formations in this area are part of the Mississippian System,

which extends northward from northern Indiana and northwestern Ohio to cover most

of the northern counties of Michigan’s Southern Peninsula. The system is largely

dominated by shallow marine terrigenous detritus (mostly shale), followed by

sandstones, and then carbonates and evaporates (Harrell et al, 1991). Several bedrock

formation subcrops within the study area such as the Marshall Sandstone, Coldwater

Shale, Bayport Limestone and Michigan Formation (Figure 2).

Coldwater Shale. The Coldwater Shale is located in the southwest part of the

study area. The Coldwater Shale subcrops predominantly in Kalamazoo County.

However, Coldwater Shale also exists in Calhoun County, as well as a small portion

in Barry County (Figure 2). The Coldwater Shale is mostly gray to bluish shale and

9

Figure 2. Bedrock geology, south-central portion of the Lower Michigan Peninsula.

Counties are outlined in black and labeled.

10

can be found interbedded with limestone and dolostone (Harrell et al, 1991).

According to Dorr and Eschman (1970) the fine-grained mud of the Coldwater Shale

was deposited at the beginning of the Early Mississippian after the Lower Peninsula

became an offshore marine environment.

Marshall Sandstone. The Marshall Formation is located directly northeast of

the Coldwater Shale and it crosses through Calhoun and Barry Counties (Figure 2).

The Marshall Sandstone is mostly formed by gray, pink and red sandstones and

siltstones, with an abundant clay matrix (Dorr and Eschman 1970; Harrell et al, 1991).

The Marshall Sandstone was deposited after a major regression in the seas at the

closure of Early Mississippian (Dorr and Eschman 1970).

Michigan Formation. The Michigan Formation directly overlies the Marshall

Sandstone. In the area of study, this formation can be found in Barry County (Figure

2). According to Dorr and Eschman (1970), the Michigan Formation is a marine

deposit of shale, gypsum, dolomite, limestone and small intervals of sandstone, which

was formed in the Late Mississippian by a transgression of the seas in Michigan. The

gray shale of the Michigan Formation is usually intebedded with sandstone in the

southern and central part of the basin, and carbonates and evaporate interbeds in the

west and north section (Harrell et al, 1991).

Bayport Limestone. The Bayport Limestone is the youngest of the

Mississippian rocks and is located to the northeast between the Michigan Formation

and the Saginaw Formation (Pennsylvanian). In the area studied, it can be found in

Barry and Calhoun Counties (Figure 2). It is comprised mainly of “Gypsiferous,

11

cherty, sparsely fossiliferous dolostone interbedded with some sandstone” (Harrell et

al, 1991).

Wisconsin Glaciation in Michigan

The last glaciation had a tremendous impact on modern topography and

glacial landforms of southwestern Michigan. This process began in the Pleistocene

approximately 2 million year ago, when the climate in the northern part of the

continent changed. During this period, glaciers advanced and retreated about twenty

times until their last major advance and retreat, called the Wisconsinan Glaciation

(Farrand, 1988). During this period, the Laurentide Ice Sheet experienced its biggest

expansion in North America.

The Wisconsin glaciation is divided into three sub episodes: the early

(Ontario), Middle (Elgin) and the Late (Michigan), based on the extent of the ice

margins (Johnson et al., 1997). During the early sub episode of the Wisconsin

glaciation between 65,000 – 79,000 yr. BP, ice advanced from the northeast and

dammed a lake in the Ontario Basin (Karrow 1984; Larson et al., 2001). Later during

the middle sub episode, between 65,000 and 35,000 yr. BP, the ice sheet extended

from the Ontario Basin to somewhere near the Finger Lakes region of New York,

where it terminated in a proglacial lake (Karrow 1984; Larson et al., 2001). Finally

came the late Wisconsin sub episode, between 35,000 and 10,000 yr. BP (Larson et

al., 2001).

12

The late Wisconsin was characterized by a series of major and minor advances

and retreats of the ice sheet (Grimley 2000; Larson et al., 2001). This period was one

of the most significant episodes because it is when all or most of the drift deposits in

the Lower Peninsula of Michigan were deposited during and following the Late

Glacial Maximum. After the Late Glacial Maximum, approximately 20,000 14

C BP,

the margin of the Laurentide Ice Sheet advanced in a series of sub lobes which at

some point covered the entire Great Lakes watershed (Dyke et al., 2002, Larson et al.,

2001, Ewald 2012). Three major lobes developed over Michigan: the Lake Michigan,

Saginaw, and Huron- Erie Lobes (Figure 3).

After the Late Glacial Maximum, the southern margin of the Laurentide Ice

Sheet began a general retreat northward into the Great Lakes watershed (Larson et al.,

2001). The Saginaw Lobe was the first of the three major lobes to readvance into

Michigan and northern Indiana (Kehew et al., 2005). The lobes were asynchronous,

and when the Saginaw Lobe began to wane or retreat the Lake Michigan and Huron-

Erie lobes advanced (Kehew et al., 2005) (Figure 3). The Kalamazoo Moraine is a

result of this interaction between the Saginaw and Lake Michigan Lobes. This

moraine appears to represent a prominent ice-marginal position and is attributed to

the Saginaw and Lake Michigan Lobe (Kehew et al., 2005). This current study is

concerned with glacial landforms and sediment deposited by the Saginaw Lobe in

Lower Peninsula of Michigan.

13

Figure 3. Interaction between the Saginaw, Huron-Erie, and Lake Michigan Lobes

(Kehew et al., 2005). Re-advance of the Saginaw Lobe after LGM approximately

21,000 yr BP (left). Retreat of the Saginaw Lobe approximately 15,000 – 16,000 yr

BP (right).

14

Saginaw Lobe Landsystems

Few studies have examined the Saginaw Lobe glacial landforms and even

fewer have attempted to characterize its subsurface deposits. A general classification

was made by Colgan et al (2005), who mapped the landsystems of the entire southern

Laurentide Ice Sheet margins. Recently, based on this classification, Kehew et al

(2012a) divided the surficial deposits of the Saginaw Lobe into four distinct

landsystems according to their morphology and depositional relationships (Figure 4).

Cores analyzed in this research will serve to correlate the glacial deposits with glacial

advances/retreat through these landsystems.

Landsystem 1 is composed of the Sturgis Moraine, which is a

terminal/recessional moraine, and a drumlinized till plain to the northeast. The Sturgis

Moraine is composed of glaciofluvial sediment with thick alluvial fans that slope off

the moraine (Kehew et al. 2012a). Tunnel valleys are present in this landsystem,

cutting and extending beyond the moraine. The drumlinized till plain is mostly

formed from sandy diamicton and is bounded by the bedrock contact of the

Coldwater Shale and overlying Marshall Sandstone to the north (Dodson, 1985;

Kozlowski, 1999, Kehew et al 2012a, Ewald 2012). Cores CA-11-01 and KA-13-01

were both drilled south of the Kalamazoo Valley on drumlins.

Landsystem 2 is bounded by of the Thornapple Valley in the north, the

Kalamazoo Valley in the south and contains the Kalamazoo Moraine. The Thornapple

Valley, a west flowing river valley, served as a channel to carry meltwater from the

15

Huron-Erie lobe (Kehew et al. 2012a). The Kalamazoo Valley, a major trench like

valley, begins as a network of tunnel valleys incised into the limestone bedrock with a

floor covered by numerous glacial boulders which are a product of the down cutting

of the overlying glacial drift (Kehew et al. 2012a; Kozlowski et al. 2005).

Landsystem 2 is mainly dominated by the Kalamazoo Moraine, which was first

described by Leverett and Taylor (1915), and it includes in its topography a

subglacial element, like tunnel valleys and eskers, which are covered by supraglacial

sediment. The landforms and sediments are believed to be the product of ice

stagnation and collapse, and include hummocks, kames and ice – walled lake plains

(Kehew et al. 2012a). Cores BA-10-02 and KA-12-02 were drilled in landsystem 2.

Landsystem 3 is located north of Thornapple Valley. The area is mainly

composed of open tunnel valleys and eskers. The Thornapple Valley is interpreted to

have carried meltwater from the Huron-Erie to the east (Kehew et al. 2012a). Core

BA-09-02 was drilled in this landsystem north of the Thornapple River Valley.

Landsystem 4 is mainly composed of recessional moraines formed from

backwasting of the Saginaw Lobe. For this research the area studied only covers

landsystems 1, 2 and 3.

16

Figure 4. Landsystems of the Saginaw Lobe according to Kehew et al (2012a),

Southern Peninsula of Michigan. Red lines represent the western boundary of the

Saginaw Lobe. Boundaries between landsystems are represented by black lines.

17

CHAPTER IV

GEOCHRONOLOGY

Glacial Geochronology in Michigan

Geochronology of glacial events in Michigan was the subject of much

speculation before the development of Carbon 14 (14

C) radioactive dating methods in

the mid 1940’s. The 14

C method enabled the dating of organic material up to a

maximum of about 50,000 to 70,000 years old. As result of this technology, portions

of the Wisconsinan glacial time scale can be accurately dated. Sadly, organic material

from older glacial time like, the Illinoian deposits can’t be dated because the age limit

goes beyond the reach for 14

C dating (Dorr and Eschman 1970).

Some studies have been conducted in an attempt to accurately date glacial

advances/retreats from different glacial landforms. Organic remains, buried by till or

outwash, have assisted in dating some of these glacial advances (Dreimanis, 1977).

Moraines or sediments associated with moraines have been extremely useful for

radiocarbon dating. The 14

C methods have provided both maximum and minimum

ages to sediments below, within, and above the moraines (Briner, 2011). One of the

oldest glacial deposits dated in Michigan thus far corresponds to an unweathered,

unnamed till unit beneath the John Ball State Park organic bed in Grand Rapids.

Samples from this organic bed yielded 14

C ages between the ranges of 39,900 to

51,000 yr. BP (Zumberge and Benninghoff, 1969; Eschman and Mickelson 1986).

18

The unnamed till was thought to be from the early to middle Wisconsin age and is

believed to antedate deposition of the organic sediment by a short interval of time

(Eschman and Mickelson, 1986). According to Dreimanis (1977) such dates are rare,

especially for the interval between 13,000 and 17,000 B.P. which is close to the Late

Glacial Maximum. Recent studies from Colgan (2013) and Lingle (2013) dated a new

organic deposit beneath Hemlock Crossing Park in Ottawa. The organic sands were

located between two till unit from core OT-12-01 and yielded 14

C ages between the

ranges of 41,920 to 42,950 yr. BP. This implies, according to Colgan (2013), that

there is a significant amount of glacial sediment older that ~42,000 yr. BP around the

area of Ottawa and surrounding counties.

Most of the radiocarbon dating made on glacial landforms has been conducted

on wood surfaces or other plant remains. Diamicton (till) unit have only been directly

dated recently (Kehew et al, 2009). This study will obtain some radiocarbon dates on

till units from three rotosonic boreholes; BA-09-01, BA-10-02 and OT-12-01, and use

these dates to correlate the till units. Core BA-09-01 was analyzed by Ewald (2012)

and OT-12-01 by Lingle (2013), for their master’s thesis.

Radiocarbon Dating on Glacial Till: Main Concerns

Glacial deposits like diamicton document glacial advances and/or retreats.

Therefore, performing studies obtaining radiocarbon dates of diamicton units

represents a potential source of information about glacial events. However, there are

several potential problems regarding dating organic matter in soils. One of the main

19

problems in dating soil bulk organic carbon is that the 14

C ages obtained are too

young due to contamination by recent contribution of carbon. The formation of soil

organic matter is an ongoing process, in which fresh carbon is continuously

incorporated at different rates and in any size fraction (Wang et al. 1996). Because of

this, 14

C dates have been interpreted as minimum ages (Perrin et al., 1964;

Scharpenseel, 1971a,b, 1972, 1976; Cherkinsky and Brovkin, 1991, Wang et al. 1996).

The landscape in the Lower Peninsula of Michigan consists mainly in glacial

drift, and organic carbon in these sediments is concentrated in the diamicton units

(Kehew et al, 2009). The Lower Peninsula of Michigan has been subject to several

glacial advances/retreat during the late Wisconsinan and multiple sources of organic

carbon are present in the glacial drift; mid-Wisconsin wood, late-Wisconsin soil and

vegetation as well as clasts of coal are also disseminated in these deposits (Kehew et

al, 2009). Mid-Wisconsin and coal organic carbon could result in bias toward older

14C ages.

Radiocarbon dates from the bulk organic carbon of diamicton could serve as

an important source of information to correlate and estimate ages in different areas,

and assist in determining past glacial events. Core KAL-03-04 analyzed by Barnes

(2007), were used to correlate dates from the boreholes analyzed in this study.

20

CHAPTER IV

METHODS

The data used in this research comes from five rotosonic cores. The cores

were drilled as parts of the Michigan Geological Survey projects funded by the U.S

Geological Survey Great Lakes Geological Mapping Coalition with the purpose of

providing more detailed analysis of glacial geology throughout the region. These

cores were then taken to the Soil Laboratory at Western Michigan University (WMU)

for grain size distribution analysis. Diamicton samples from some of the cores were

collected and taken to the WMU Engineering College Geotechnical Laboratory for

consistency analysis (Atterberg Limits). Samples for 14

C dating were also collected to

be pretreated in the Geosciences Dept. Isotope Laboratory and have then sent to the

DirectAMS Laboratory in Seattle to be dated. The following methods and procedures

were used to accomplish the proposed research:

Particle Size Analysis

Five borings were chosen for textural/particle size analysis to determine the

grain size distribution. These tests were done according to the method modified from

Bowles (1978) to separate the 2µm clay particles. Sieves were selected according to

the ASTM protocol E 11. Similar techniques of analysis were used by Gardner (1997),

21

Flint (1999), Wong (2002), Beukema (2003), Barnes (2007), Woolever (2008) and

Ewald (2012). Results are presented in Appendix A.

Soil samples were taken about every 2 to 3 foot interval or when a change in

the soil layer was noted. The sample weight varies depending on the water content at

the time of collection and grain size distribution, but approximately 400 to 500 g of

sample was collected. As stated above, two sieving methods were used depending on

the type of samples: for coarse samples, the dry sieve method and for fine samples,

the wet method. The following procedure was used to analyze the grain size

distribution in coarse samples:

1. Approximately 400 to 500 grams of the sample was collected, placed in an

aluminum pan and dried in the oven at 105oC for at least 24 hours.

2. A pestle and a porcelain mortar were used to disaggregate the dried

samples. A rubber tip pestle was used to gently disaggregate the sample

(porcelain pestle was used for sample with high clay content). After this

the sample was weighed.

3. Seven sieves were stacked in order from: #5, #10, #18, #35, #60, #120,

#230 and bottom pan (order from the coarsest to the finest).

Approximately 400 grams of the disaggregated sample was poured into the

stack of sieves and covered with a top pan.

4. The stack of sieves was placed in the Ro-tap mechanical sieving device to

be agitated for 10 minutes.

22

5. After 10 minutes, the amount of particles retained in each sieve was

weighed and recorded.

6. The fines (silt and clay) from the bottom pan were stored in the oven and

then separated using the gravitational separation method based on Stokes’

Law (Hillel, 1998).

The following sieving procedure was used to analyze the grain size

distribution in samples with high content of clay and silt:

1. Approximately 400 to 500 grams of sample was collected, placed in an

aluminum pan and dried in the oven at 105oC for at least 24 hours.

2. The sample was disaggregated with a porcelain pestle and about 450

grams were taken and poured in a metal cup with tap water.

3. The sample in the metal cup was then agitated in a sediment stirrer

machine for 1 minute, then with a stir rod for another minute and washed

through a #230 sieve with a bottom pan to separate sand and gravel from

clay and silt.

4. The sample remaining in the #230 sieve was the sand and gravel. The

content was then rinsed in a separate container and allowed to dry in the

oven to be sieved again using the dry method explained above.

5. The sample captured in the bottom pan was the clay and silt. The content

was then rinsed into a separate container and dried in the oven at 105oC

for at least 24 hours. After drying, the sample was then mixed with the

23

fines that remained from the sieving of the sand and gravel portion. From

this mix 10 grams was collected for the silt and clay separation.

The following procedure was used for the silt and clay separation (modified

by Ewald, 2012):

1. Approximately 10 grams of the sample fines were collected and placed in

a 1000 ml beaker (if the sample was less than 10 grams, then the entire

sample was used).

2. An alkaline solution of 0.5% sodium hexametaphosphate (Na6O18P6) was

made to act as a deflocculant, and 700 ml of this solution was poured in

the beaker already containing the 10 gram sample.

3. The sample with the solution was then agitated in a sediment stirrer

machine for 10 seconds and then placed in an ultrasonic vibration device

for 20 minutes.

4. After 20 minutes, the sample was allowed to settle for 2 hours (120 min),

during this time the clay particles remained in suspension while the silt

settled to the bottom of the 1000 ml beaker.

5. After 2 hours the suspended clay and the settled silt were poured into

separate weighed aluminum pans and placed in the oven at105oC for 24

hours. The next day the weight of the aluminum pans was recorded.

24

Figure 5. The Wentworth grain-size scale for sediments: Wentwoth size classes,

phi (Ø) units and U.S Standard sieve (modified from USGS, 2006)

Sieve Size

ASTM No.

(mm) (Ø) (U.S. Standard)

4.0 -2 5 Pebble Gravel

2.0 -1 10 Granule

1.0 0 18 Very Coarse

0.500 1 35 Coarse

0.250 2 60 Medium

0.125 3 120 Fine

0.063 4 230 Very Fine

0.031 5 Coarse

0.015 6 Medium

0.008 7 Fine

0.004 8 Very Fine

0.002 9 Clay

Class

Sand

Silt

Particle Length

P

a

n

Grade

25

Atterberg Limits

The Atterberg Limits were used to determine the clay consistency in 18

diamicton samples from three of the five borings. These borings were chosen based

upon location (landsystem), and relevance to the study. The test was performed

according to the American Society for Testing and Material (ASTM, 2010) protocols

to measure moisture content at which the sample changes from semi-solid to plastic

state (Plastic Limit) and from plastic to liquid state (Liquid Limit). Engineers have

been using this test since the 1900s for correlations of physical soil parameters and

soil identification (Das, 2010). Casagrande (1932) conducted several studies using the

liquid limit to correlate the plasticity index (PI) of different soil types. The following

procedure was used to prepare the samples for the liquid and plastic limit test:

1. Approximately 200 grams of the sample was taken and disaggregated

using a porcelain pestle and mortar.

2. The sample was poured in a #40 sieve with a bottom pan and sieved. This

process was repeated until about 120 to 200 grams of sample was retained

in the bottom pan.

3. The sample was weighed, recorded and then poured into a porcelain dish

for liquid and plastic limit test.

The liquid limit (LL) according to the ASTM (2010) is determined by

performing trials in which a portion of the soil sample is spread in a brass cup and a

groove is cut at the center with a grooving tool. Then with a mechanical device the

26

cup is lifted and then dropped until the groove is closed (Figure 5). The number of

drops and the moisture content is then recorded. The method used was the ASTM

One-Point Liquid Limit - Method B. The following procedure (ASTM, 2010) was

used to prepare the samples for the liquid limit (LL):

1. Deionized water was poured into the sample then thoroughly mixed until

the consistency to close the groove was between 20 and 30 blows. If the

number of blows exceeded 30 or was lower than 20, the sample was

removed from the brass cup and the water content was adjusted.

2. After getting a number of blows between 20 and 30, a portion of the

samples (from the closed groove) was removed to measure the water

content, then the soil from the brass cup was removed, then remixed in the

dish and a new sample is placed in the cup.

3. A second test was then made until the sample required the same number of

blows to close the groove as the first test or the difference in the number

of blows was equal to two. A portion of the sample was then removed to

measure the water content.

4. The Liquid Limit (LL) is the average of the two tests (to the nearest whole

number).

5. If the difference in values equal 1% the test had to be repeated.

The plastic limit (PL) according to the ASTM (2010) is determined by rolling

(in a ground - glass plate) a small portion of soil into a 3.2 mm diameter thread until

its water content is reduced to a point at which the thread crumbles and can no longer

27

be pressed together and rerolled. The following procedure was used to prepare the

samples for the plastic limit (PL):

1. From the soil prepared for the liquid limit test, a 20 gram sample was

selected, reducing the water content to a consistency in which it could be

rolled without sticking to the hand or the glass plate.

2. From the 20 grams, 2 grams were extracted and turned, by hand, into an

ellipsoidal mass. The ellipsoidal mass was then placed in the glass plate

and rolled until its diameter reached 3.2 mm.

3. When the samples had a 3.2 mm diameter, they were then broken into

three pieces and squeezed together, reformed and turned into an ellipsoidal

mass and rerolled again until the thread crumbled and could not be

reformed into an ellipsoidal mass and rolled again.

4. The Plastic Limit (LL) is the average of two tests (to the nearest whole

number). If the difference in values is equal or greater than 1.4% the test

had to be repeated.

28

Figure 6. Clay consistency and Particle size analysis tools. Brass cup and a groove

used for liquid limit (Left). Stack of sieves used for particle size distribution analysis

(Right).

29

Bulk Organic Carbon Assay

The bulk organic carbon assay was used to extract the carbon dioxide from the

diamicton units. The amount of organic carbon was then calculated and the carbon

dioxide was sent to DirectAMS Laboratory in Seattle for Carbon 14 dating. About 14

organic carbon samples were analyzed in the Stable Isotope Laboratory of the

Geosciences Department at Western Michigan University, from which 6 were

selected for Carbon 14 dating. The preparation procedure is listed below:

Inorganic carbon removal:

1. Approximately 7 grams of the sample was taken and disaggregated using a

porcelain pestle and mortar.

2. The sample was poured into a 15 mL plastic centrifuge tube, filled with

6N Hydrochloric acid (HCl), agitated and allowed to sit for 24 hours.

3. The next day, the sample was centrifuged for a total of 20 minutes; the

first 10 minutes at ½ speed and the next 10 minutes at ¾ speed.

4. After centrifugation, the acid was decanted into a waste container,

replaced with new acid and allowed to rest for 24 hours. This step was

repeated 4 to 5 times.

5. After the last centrifugation, the acid was decanted and replaced with

deionized water to remove the acid from the samples.

30

6. The samples were then agitated and centrifuged for a total of 20 minutes;

10 minutes at ½ speed and 10 minutes at ¾ speed. The deionized water

was then replaced.

7. Step 6 was repeated until the samples pH turned neutral (around 7), using

a pH indicator.

8. Once the samples pH turned neutral, the water was decanted in a waste

container and the sample were left drying in an oven at a temperature of

38 0C.

Sample Combustion and CO2 extraction:

1. Approximately 500 mg of the dry sample was taken and disaggregated.

2. The dry sample was poured into a 6 mm Quartz tube. The 6mm tube was

then placed inside a 9 mm Quartz tube with 1 gram of cupric oxide.

3. Air inside the 9 mm tubes was extracted on one of the vacuum lines. The 9

mm tube was then sealed with a blowtorch.

4. The 9 mm tube was then placed in the furnace and combusted for 3 hours

at a temperature of 900 0C.

5. The combusted sample was mounted onto an extraction unit in a vacuum

extraction line. The 9 mm was then broken releasing the CO2 gas into the

extraction unit and then to the vacuum line.

6. Liquid nitrogen was used to capture the CO2 gas in the U-shaped tube of

the vacuum line and release other gases like Nitrogen.

31

7. The liquid nitrogen was removed from the U-shaped tube and replaced

with a slush made with dry ice and alcohol (at 70 oC). This released the

CO2 gas trapping the moisture and water. The CO2 gas was then capture in

a 10 cm tube of the vacuum line with liquid nitrogen.

8. The liquid nitrogen was removed, releasing the CO2 gas inside the 10 cm

tube. The reading in the pressure gauge was then recorded to calculate the

amount of CO2 gas in the tube (micromoles).

9. A sample tube was added to collect the CO2 gas. Liquid nitrogen was used

in the sample tube to capture the CO2 gas.

10. The δ13

C of gas was then measured in a Mass Spectrometer. The gas was

returned to the vacuum line, sealed in a 9 mm Pyrex tube with a blowtorch

and set to DirectAMS for Carbon 14 dating.

Inorganic Carbon Assay

The inorganic carbon assay was used to extract the carbonates from the

diamicton units. Six samples were pretreated in the Stable Isotope Laboratory of the

Geosciences Department at Western Michigan University and then sent to the Stable

Isotope Laboratory from Oklahoma State University for isotope analysis. The

preparation procedure is listed below:

1. Approximately 20 mg of the sample was taken and disaggregated using a

porcelain pestle and mortar.

32

2. The sample was then poured into blood tubes. In addition, a 9 mm Pyrex

tube was glued inside the blood tube.

3. After the glue between the tubes was dry, Phosphoric acid (H3PO4) was

injected in the 9 mm tube glued to the blood tube. The blood tube was then

sealed with a plastic cap.

4. Air inside the blood tube was extracted on one of the vacuum lines and

then was taken to the water bath. The water bath was used to avoid 18

O

fractionation.

5. Then the next day, acid and sediment sample were mixed inside the blood

tube and the CO2 gas was extracted following the same procedure as the

bulk organic carbon assay.

Maps and Cross Section Data

Maps and cross sections were created using ArcGIS software program

ArcMap 10. Data used to create the maps, including water well logs, were imported

from the State of Michigan’s Geographic Data Library and wellogic data base, with

the exception of the rotosonic cores drilled in the field. This database is accessible on

the State of Michigan website. The data was translated into uniform lithological terms.

All of the lithological terms including the borehole data were combined into three

categories based on the grain size distribution (Table 2).

Lithologies were grouped as “Sand & Gravel” (yellow), “Silt & Clay” (blue)

and “Diamicton” (green). Clayey units mixed with gravel and/or sand were

33

interpreted as diamicton. This procedure is also used by the U.S Geological Survey

and recently by Ewald (2012). Bedrock topography data was obtained from Mr. John

Esch of the Michigan Department of Environmental Quality.

Table 2

Interpreted Water Well Lithology

Water Well Logs Uniform Lithology Color

Clay Silt & Clay Blue

Clay & Sand Silt & Clay Blue

Clay & Silt Silt & Clay Blue

Sand & Silt Silt & Clay Blue

Muck Silt & Clay Blue

Marl Silt & Clay Blue

Gravel Sand & Gravel Yellow

Gravel & Boulders Sand & Gravel Yellow

Gravel & Clay Sand & Gravel Yellow

Gravel & Sand Sand & Gravel Yellow

Sand Sand & Gravel Yellow

Hardpan Diamicton Green

Clay & Stones Diamicton Green

Clay & Boulders Diamicton Green

Clay & Gravel Diamicton Green

Clay Gravel Sand Diamicton Green

Clay Gravel Stones Diamicton Green

Clay Sand Gravel Diamicton Green

34

CHAPTER V

RESULTS

Several cores were drilled within the Saginaw lobe terrain in the Michigan

Southern Peninsula. These cores are described according to the landsystem in which

they were drilled. A textural classification system is used to express the general

characteristics in the borehole soils. Sediment textures for the cores BA-09-02, BA-

10-02, CA-11-01, KA-12-02 and KA-13-01 are classified using the U.S. Department

of Agriculture (USDA) textural classification method.

Landsystem 3: North of the Thornapple Valley

Cores BA-09-02 was drilled north of the Thornapple River Valley in a

northeast -southwest trending tunnel valley in Barry County. The area is located

within the range of landsystem 3 (Figure 4). Textural analysis was completed by

Ewald (2012) and is replotted in Figure 6.

BA-09-02

The stratigraphy in the core is composed mainly of diamicton and fine

sediments. The total depth of the core was -63.1 meters (207 feet) and it reached

bedrock at -57 meters (187 feet). Bedrock, in this area, comes from the Michigan

Formation (Figure 2), which is mainly shale. Three diamicton units are present below

a depth of 16.3 meters, separated by two thick layers of silt and clay. The

predominant particle fraction in this core is silt and clay (Figure 7).

35

The interval between 0 (surface) to -7 meters has two layers, one of sand and

one of gravelly sand (Figures 7, 8). The first layer (0.4 m) is a sandy loam consisting

mainly of sand, with an average normalized texture of 51.5% of sand, 34.1% silt and

14.4% clay. The gravelly sand unit is mostly coarse; clay is almost nonexistent in this

layer; it is composed of about 95% sand, 3.5% silt and 1% clay. The sand unit is

made up of mostly fine sand.

Between -7 to -16 meters is located a silty clay bed with an average

normalized texture of 1.2% sand, 66.6% silt and 32.2% clay, underlain by a sand

and silt unit between two gravelly sand layers (Figures 7, 8). The first gravelly sand

layer is formed by very coarse material with some sand, while the second is a mixture

of gravel, sand and silt.

The interval between -16 to -46 meters has two diamicton units separated by

two layers; a silt unit and a silty clay unit (Figures 7, 8). The upper till unit (Unit A-1)

is a uniform/compact clay loam diamicton with an average texture of 32.3% sand,

41.6% silt and 26.1% clay. The middle till (Unit A-2) has an average texture of

27.7% sand, 43.4% silt and 28.9% clay. The unit is very similar to the previous layer,

being comprised of a clay loam diamicton, uniform and compact, but with a higher

percentage of fines and a lower percentage of coarse particles. At -46 m, there is a

bed of sand separating part of the middle till unit, which could mean that the till unit

below the sand bed is not part of the middle till unit (Figures 6, 7).

36

Figure 7. Logplot Diagram of BA-09-02 showing lithology, gamma ray signature, and

grain size distribution. The core contains two thick diamicton units separated by

lacustrine sequences. The bedrock is shale from the Michigan Formation.

37

Figure 8. Matrix texture (<2.00 mm) of all samples in BA-09-02. Green circles

represent diamicton, blue circles represent silt/clay and yellow circles represent

sand/gravel. The upper diamicton (Unit A-1) consists of sand and silt, with an

average texture of 32.3% sand, 41.6% silt and 26.1% clay. The middle diamicton

(Unit A-2) is dominated by silt and clay, with an average texture of 27.7% sand,

43.4% silt and 28.9% clay.

38

The till below the sand bed is a clay loam diamicton similar to the previous till units.

The last layer is between -47 and 54 meters and consists of a silty clay unit. This silty

clay layer is formed of an equal amount of fines with an average texture of 0.7% sand,

51.4% silt and 48% clay.

Landsystem 2: South of the Thornapple and North of the Kalamazoo Valleys

Two cores BA-10-02 and KA-12-02 were drilled south of the Thornapple

River Valley and north of the Kalamazoo River Valley. The boring BA-10-02 was

drilled in Barry County and KA-12-02 in Kalamazoo County. The area is located

within the range of landsystem 2 (Figure 4). The glacial features in this area include

the Kalamazoo Moraine between the Thornapple River Valley to the north and the

Kalamazoo Valley to the south.

BA-10-02

The stratigraphy in the core is composed mainly of diamicton, sand and silt

(Figure 9, 10). The boring was drilled to a depth of -85 meters (279 feet) and reached

bedrock at -73.15 meters (240 feet). The bedrock in this area is shale and comes from

the Michigan Formation (Figure 2). About three thick diamicton units are present in

the core. The first two units are coarse grained and the deepest one is finer.

Between 0 (surface) to -13 meters are interbedded sand and silt/clay in the

first four meters, followed by a unit of sandy diamicton interbedded with gravel

(Figures 9, 10). The diamicton (Unit B-1) is a sandy loam with an average texture of

39

66.7% sand, 25.1% silt and 11.1% clay. Sand and gravel lenses are present in the

middle and base of this till unit.

The interval between -13 to -36 meters is mostly dominated by sandy

sediments. The first six meters consist of a sandy loam, followed by a silt layer

(Figures 9, 10). The sandy loam has an average texture of 82.6% sand, 15% silt and

2.4% clay. The next five meters is comprised mainly of sand with a thin bed of silty

clay. Below this bed is the second diamicton unit (Unit B-2), a compact sandy loam

with gravel. This unit has an average texture of 77.6% sand, 18.1% silt and 4.3% clay.

Four meters of sand with some gravel are present below the diamicton.

In the interval between -36 to -66 silt fractions start to dominate (Figures 9,

10). A sandy loam unit is present in the first 8 meters, followed by a silt layer in the

next 10 meters. The sandy loam has an average texture of 55.7% sand, 38.7% silt and

5.6% clay. Interbedded diamicton (Unit B-3) with variable textures is present in the

interval -54 to -66 meters. A gravelly/sandy loam diamicton is located between -54

and -58 meters, with an average texture of 58.4% sand, 30.7% silt and 11% clay. A

gravel layer separates the second diamicton bed into upper and lower units. This part

is a clay loam diamicton formed mostly by 30.7% clay and 47% silt. The third

diamicton bed is separated by a silt layer. This bed consists mainly in sand and silt

with an average texture of 40.5% sand, 40.4% silt and 19% clay.

The last interval between -66 to -73 meters is mainly sand and diamicton

(Figures 9, 10). The first 5 meters are composed of interbeded sand and silt.

40

Figure 9. Logplot Diagram of BA-10-02 showing lithology, gamma ray signature, and

grain size distribution. The core contains three thick diamicton units separated by

sandy and silty lacustrine sequences. The bedrock is shale from the Michigan

Formation.

41

Figure 10. Matrix texture (<2.00 mm) of all samples in BA-10-02. Green circles


sand/gravel. Upper diamicton units (Unit B-1, B-2) consist mainly in sand and silt

with an average texture ranging from 58.4% - 77.6% sand, 18.1% - 30.7% silt, 4.3% -

11.1% clay. The lower diamicton unit (Unit B-3) is mainly formed by silt and clay

with an average texture ranging from 22.3% - 40.5% sand, 40.4% - 47.0% silt, 19.0%

- 30.7% clay.

42

Underneath this layer is another diamicton bed. This bed is mainly a clay loam

diamicton, with 22.5% of gravel. The average normalized texture for this unit is 30%

sand, 42.1% silt and 27.9% clay. This unit is believed to be part of the shale bedrock.

KA-12-02

The boring was drilled to a depth of -81 meters (266 feet) and reached

bedrock at -79 meters (259 feet). The bedrock in this area is shale and comes from the

Michigan Formation (Figure 2). The stratigraphy in this core is diverse, but mostly

sand and gravel followed by intercalated silt and clay (Figures 11, 12). A diamicton

unit is located between thin sand lens in the intervals of -16 and -30 meters. The unit

is mainly fine graineds.

Interval 0 (surface) to -14 meters. The first 5 meters in this core are mainly sand,

followed by 6.5 meters of gravel. A thin bed of diamicton is present below the gravel.

This unit has an average texture of 50.3% sand, 22.5% silt and 27.2% clay. The final

interval is mostly made up fines; a silt layer is below the diamicton unit, followed by

a clay loam. The gravel percentage in these layers is below 1% (Figures 11, 12).

Interval -14 to -45 meters. A thick diamicton unit (Unit C-1) is lies between

two small layers of sand. The unit is 13 meters thick and has a loam texture with an

average normalized texture of 49.5% sand, 34.9% silt and 15.5% clay. The content of

gravel is less than 5 %, and is the only diamicton unit in this core.

43

Figure 11. Logplot Diagram of KA-12-02 showing lithology, gamma ray signature,

and grain size distribution. The core contains one thick diamicton unit. Lacustrine

sequences are present above the diamicton unit and between 49 and 65 meters. The

shale bedrock underlies thick coarse sediments.

44

Figure 12. Matrix texture (<2.00 mm) of all samples in KA-12-02. Green circles


sand/gravel. The diamicton unit (Unit C-1) in this core has a mean texture of 49.5%

sand, 34% silt and 15.5% clay.

45

From a depth of -30 to -45 meters the core shifts from silty and clayey to sandy and

gravelly. Intercalated sand and gravel with some silts dominates this interval (Figures

11, 12).

The stratigraphy changes two more times between the depths -45 and -79

meters, first from sand to silt/clay and then, to gravelly sand followed by 3 meters of

gravel. The interval begins with a silt unit followed by a fine sand layer, at -48 meter

this setting changes to interbedded of silt/clay, and then to interbedded sand/silt.

Finally the core becomes coarser at -65 meters, with 10 meters of gravelly sand,

followed by 3 meters of gravel (Figures 11, 12).

Landsystem 1: South of the Kalamazoo Valley

Two cores, CA-11-01 and KA-13-01, were drilled south of the Kalamazoo

River valley. Core CA-11-01 was drilled on a drumlin, within the city of Battle Creek

in Calhoun County. Core KA-13-01 was also drilled on a drumlin, but south of the

Kalamazoo Valley and southeast of the city of Portage, Kalamazoo. Both cores fall

within the area of landsystem 1 (Figure 4).

CA-11-01

The stratigraphy in this core is composed mainly of diamicton. The boring

was drilled to a depth of -54.6 meters (179 feet) and reached bedrock at -54 meters

(177 feet). Bedrock in the area is siltstone of the Marshall Formation (Figure 2). Four

46

diamicton units are present in this core, separated by thick units of coarse sediments.

The predominant particle size fraction is mainly coarse (Figures 13, 14).

The first interval goes from 0 (surface) to -19.5 meters, and is mainly a sandy

loam diamicton. The diamicton unit (Unit D-1) has an average normalized texture of

68.9% sand, 22.1% silt, and 9.0% clay. The unit becomes more gravelly at greater

depths, with an average of 7.5% gravel in the upper section and 16.2% between the

middle and bottom sections. An interbedded unit of sand and gravel is present

between -3 and -6 meters. Below the diamicton, 1.5 meters of fine sand is present and

its marks a shift from sand to silt (Figures 13, 14).

Between -19.5 and -31 meters is the second diamicton unit (Unit D-2). One

meter above the diamicton, two beds, one of sandy loam and one of silt are present.

The sandy loam has an average normalized texture of 59.2% sand, 35.2% silt and

5.6% clay. A small bed of silt lies directly below the diamicton, followed by 4 meters

of gravel and another small bed of silt. The dimicton in this interval is a sandy loam

unit, with about 11.1% gravel and an average normalized texture of 60.1% sand,

28.5% silt and 11.4% clay (Figures 13, 14).

The interval from -31 to -41 meters is dominated mainly by gravel and sand.

Interbedded diamicton (Unit D-3) and gravelly sand is present in the first 5 meters,

followed by 4 meters of gravel. The last meter is occupied by a silt/sand layer.

Diamicton in this interval is a sandy loam unit with an average normalized texture of

66.5% sand, 21.6% silt and 11.9% clay. The amount of gravel in this diamicton unit is

an average of 11.1% (Figure 13, 14).

47

Figure 13. Logplot Diagram of CA-11-01 showing lithology, gamma ray signature,

and grain size distribution. The core contains four thick diamicton units separated by

sand and gravel. Sand and gravel between diamictons are poorly sorted, and are

interpreted as outwash deposits. The bedrock is siltstone from the Marshall Formation.

48

Figure 14. Matrix texture (<2.00 mm) of all samples in CA-11-01. Green circles


sand/gravel. Diamicton units in this core have a high amount of gravel and sand. The

mean texture of the upper two diamictons (Unit D-1, D-2) are 68.9% sand, 22.1% silt,

9.0% clay, and of 59.2% sand, 35.2% silt, 5.6% clay. The lower two diamictons

(Unit D-3, D-4) have a mean texture of 66.5% sand, 21.6% silt, 11.9% clay and

40.8% sand, 40.4% silt, 18.8% clay.

49

The last interval, between -41 to -54 meters, is mainly diamicton finer than the

upper till unit (Figure 13, 14). The diamicton unit (Unit D-4) is divided at -50 meters

by 1.5 meter of silt, and above the unit, 4 meters of gravelly sand. The first diamicton

in this interval is a loam unit with an average normalized texture of 40.8% sand,

40.4% silt and 18.8% clay. Gravel percentage is low in this unit, about 1.8%. The

second diamicton is another sandy loam unit, located beneath the silt layer. The

average normalized texture is about 71.3% sand, 23.6% silt and 5.2% clay.

KA-13-01

The stratigraphy in this core is composed of more than 70% sand/gravel, and

sandy diamicton. The boring was drilled to a depth of -48.5 meters (159 feet) and

reached bedrock at -47 meters (154 feet). Bedrock in the area is shale of the

Coldwater Shale (Figure 2). At least two diamicton units are present in this core,

separated by thick layers of coarse sediments. The predominant particle fraction is

gravel, followed by sand (Figures 15, 16).

A diamicton unit (Unit E-1) is located between 0 and -15 meters and it split by

a small sand bed at -6 meters. The first unit is mainly formed by loamy sand with

13% gravel and an average normalized texture of 64.0% sand, 28.4% silt and 7.6%

clay. Interbedded diamicton and gravel/sand is present beneath the small sand bed at -

6 meters. The unit is a sandy loam diamicton with an average texture of 63.5% sand,

30.6% silt and 5.8% clay. A thick gravel unit is present below the diamicton,

50

followed by another unit of sand. The gravel is about 3.5 meters thick (Figures 15,

16).

The interval between -15 and -37 meters is mainly composed of very coarse

sediment (Figures 15, 16). The first bed is composed of 6 meters of gravel, which is

very coarse with some sand; clay/silt is very low in this unit. The next 5 meters

include intercalated gravelly sands with a gravel bed between them. Interbedded sand/

gravel occupy the next 9 meters, followed by 3 meters of gravel.

The last diamicton unit (Unit E-2) is located between two sand units in the

interval that goes from -37 to -47 meters. The unit is a sandy loam diamicton, uniform

and compact, low on gravel (about 3.8%), with an average texture of 59.1% sand,

29.0% silt and 11.9% clay. The sand units above and below the diamicton are form

mostly by fine sand and some silt. Gravel is present only in a small bed above the

diamicton unit (Figures 15, 16).

51

Figure 15. Logplot Diagram of KA-13-01 showing lithology, gamma ray signature,

and grain size distribution. The core contains two diamicton unit separated mainly by

gravel with sand. The bedrock in this area is shale of the Coldwater Shale Formation.

52

Figure 16. Matrix texture (<2.00 mm) of all samples in KA-13-01. Green circles


sand/gravel. The two diamicton in this core are mainly sandy units with gravel. The

mean texture of the upper diamicton (Unit E-1) is 64.0% sand, 28.4% silt, 7.6% clay,

and the lower diamicton (Unit E-2) of 59.1% sand, 29.0% silt and 11.9% clay.

53

Diamicton Clay Consistency

The clay consistency of diamicton samples from cores BA-09-02, BA-10-02

and CA-11-01was tested with the plastic and liquid limit test (Table 3). Samples from

these boreholes are mostly inorganic clay with low to medium plasticity. The result

indicates a strong correlation between plasticity indexes in diamicton between the

depths of -46 to -72 meters. The following are the results of the plastic and liquid

limit test:

BA-09-02: According to the plasticity index, the clays in these diamictons

range from low to medium plasticity. Samples from the upper and lower diamicton

consist of low plasticity clay. Diamictons samples between the intervals -22 to -46

meters are formed by medium plasticity clay, close to high plasticity. Clay color

varies between brown and gray. The diamictons in this core contains higher clay

content. Bedrock in the area is shale, which is a possible clay source in the diamicton

(Table 3).

BA-10-02: According to the plasticity index, clay in these diamictons varies

from slight to low plasticity, close to medium plasticity in samples between -10 and

-55 meters. The clay between intervals -12 to -32 meters is slightly plastic to almost

non plastic, provably due to the high silt content in these diamictons. Silt content

becomes lower in diamictons samples close to bedrock. Clay color varies from orange

to brown and dark gray. Bedrock in the area is also shale, and this explains the dark

54

Table 3

Diamicton Clay Consistency Data Results

Sample # Depth

(meters)

Depth

(feet)

Liquid

Limit

(LL)

Plastic

Limit

(PL)

Plasticity

Index

(LL - PL)

Plasticity

Classification

BA-09-02

1-B 20 64 20 13 7 Low

2-B 22 73 24 13 11 Medium

3-B 38 126 29 15 14 Medium

4-B 42 138 32 15 18 Medium

5-B 46 152 30 13 17 Medium

6-B 56 183 19 11 8 Low

BA-10-02

1-C 10 32 17 9 8 Low

2-C 12 38 14 10 4 Slightly

3-C 29 94 14 11 3 Slightly

4-C 32 103 15 12 3 Slightly

5-C 55 181 19 11 8 Low

6-C 72 235 19 13 5 Low

CA-11-01

1-D 9 30 15 12 3 Slightly

2-D 15 50 16 12 4 Slightly

3-D 22 72 14 12 2 Slightly

4-D 25 83 14 12 2 Slightly

5-D 46 150 20 13 7 Low

6-D 47 155 25 16 10 Medium

55

gray color in the clays. Diamicton below -55 meters, near the shale bedrock has low

plasticity (Table 3).

CA-11-01: According to the plasticity index, the clays in these diamictons are

slightly plastic, approaching a value of zero plasticity between the intervals of -9 to

-25 meters. The plasticity increases from low to medium between -46 and -47 meters

depth. Clay color in these diamictons varies from light brown to gray, with gray

diamicton having the lowest plasticity. The bedrock in the area is mainly siltstone,

which doesn’t contain a clay source (Table 3).

Cross Section A-A’

Cross section A-A’ has been constructed between Barry, Kalamazoo and

Calhoun Counties and it shows the general distribution of glacial deposits from the

Saginaw Lobe (Figure 17). The cross section includes water well logs within 826

meters of the cross section line, as well as cores BA-09-02, BA-10-02, KA-12-02,

CA-11-01 and KA-13-01. Red dashed lines represent the boundaries between

sedimentary packages. Water well logs are grouped into three categories according to

grain size.

Boreholes BA-09-02 and BA-10-02. Water well logs between the cores BA-

09-02 and BA-10-02 indicate that uplands are mainly underlain by fine sediments

such as silt/clay and fine - grained sediment mixed with diamicton (Figures 17, 18).

Ewald (2012) interpreted the high silt and clay content as a possible lacustrine origin.

A few deposits of coarse sediment occur in the middle section of the profile, followed

56

Figure 17. Location of cross section A-A’. Water wells are marked with smaller blue

circles.

57

by sandy diamicton mixed with clay above the bedrock. According to the water well

logs, sediments in the Thornapple valley consist mostly of sand in the first -24 meters

and become mixed with diamicton and clay/silt until it reaches the bedrock.

Boreholes BA-10-02 and KA-12-02. Water well logs between the cores BA-

10-02 and KA-12-02 indicates diversity in the uplands stratigraphy (Figures 17, 18).

The northern section, close to core BA-10-02, consists of thick intervals of silt/clay

and fine grained sediment mixed with diamicton. The middle section contains a layer

of thick coarse sediments, which is mainly sand and gravel. The silt/clay continues

below the sand, followed by a thick interval of sandy diamicton.

Uplands on the southern section, close to core KA-12-02, are comprised of

about 50 meters of coarse sediment, followed by a thick interval of diamicton mixed

with silt/clay and sand. A small layer of sand separates some of the silt/clay from the

diamicton.

Boreholes KA-12-02 and CA-11-01. Coarse and fine sediments intercalate

between cores KA-12-02 and CA-11-01. According to the water well logs, uplands

near core KA-12-02, consist primarily of coarse sediments and sandy diamicton, then

a few meters below silt and clay start to dominate the middle section, which is

dominated by an interval of sand (Figures 17, 18). The bottom section has a layer of

silt/clay, followed by sand. Water well logs, show that The Kalamazoo Valley is

underlain mainly by coarse sediment, with silt and clay are present below the sand. It

is possible that erosion removed part of the fine sediments. Stratigraphy near core

58

Figure 18. Cross Section A-A’. Water wells and cores lithologies in landsystem 1, 2 and 3. Lithologies were grouped in 4 different categories (Silt&Clay, Sand&Gravel, Diamicton and Bedrock) for better

interpretations. Red dashed lines marks the interpreted stratum and solid gray lines the bedrock elevation.

59

CA-11-01 consists mainly of diamicton. Around -37 meters below surface coarse

sediments start to appear, followed by diamicton and clay.

Boreholes CA-11-01 and KA-13-01. Uplands in the area consist mainly in

sandy diamicton and coarse sediments deposits (Figures 17, 18). Stratigraphy near

core CA-11-01 is mainly diamicton in the upper and bottom parts. The middle part is

mostly silt, clay and fine sands. The middle-bottom section between cores CA-11-01

and KA-13-01 is mainly sand. More data is needed to draw interpretations regarding

the extent of sand in the layer in this section. Near core KA-13-01 diamicton, silt and

clay appear again in the uplands, followed by a small layer of interbedded clay and

sand. Close to the bedrock, in the bottom part, is a sandy layer with some traces of

diamicton.

Radiocarbon and δ13

C Analyses

Samples from four boreholes were analyzed in the Geosciences Dept. Stable

Isotope Laboratory, and then sent to different laboratories for Carbon 14 dating.

Samples from cores BA-09-01, BA-10-02 and OT-12-01 were dated at DirectAMS

laboratory. The last core, KA-03-04 was analyzed by Barnes (2007) (Table 6).

Organic carbon content, along with δ13

C values, were also determined in the Stable

Isotope Laboratory in the Geosciences Department (Table 4). Inorganic carbon

(carbonates), along with δ13

C and δ18

O were analyzed by the Stable Isotope

Laboratory at Oklahoma State University (Table 5).

60

δ18

O (VSMOW) analyses on carbonates collected from the samples of

diamicton ranged between 23.8 and 25.0 per mil, and δ13

C (VPDB) analyses ranged

between -2.4 and 1.3 per mil (Table 5). These δ13

C values are commonly seen in

marine sediments, which indicate carbonate deposits of marine origin. This result is

consistent with the enriched δ18

O values, which are mainly seen in the dolomite/

limestone deposits. In addition glacial deposits around southwestern Michigan overlie

Mississippian bedrock, which consists of 47% carbonates (limestone, dolomite) (Dorr

and Eschman 1970).

δ13

C analyses on bulk organic carbon collected from the diamicton samples

ranged between -23.53 and -26.53 per mil (Table 4). These values suggest the

presence of C-3 plants, which is consistent with the climate and vegetation of

southwestern Michigan. In addition, radiocarbon ages extracted from the diamicton

units bulk organic carbon give similar dates between 9 and 11 meters in three of the

core samples (Table 6). Radiocarbon ages tend to get younger between 29 and 57

meter. The bulk organic carbon in these sediments appears to be late Wisconsin in

age.

61

Table 4

Diamicton Bulk Organic Carbon Data

Footage

Core ID (meters) (feet) δ13C Mean organic

carbon (%)

BA-10-02 9 31 -25.91 0.48

OT-12-01 9 31 -25.42 0.53

KA-03-04 11 56 -27.36 0.60

OT-12-01 29 96 -26.53 0.26

BA-09-01 55 180 -25.93 0.22

BA-10-02 57 186 -23.53 0.10

Table 5

Diamicton Carbonates Data

Footage δ

13C δ

18O

Core ID (meter) (feet) (VPDB) (VSMOW)

BA-10-02 9 31 1.2 24.5

OT-12-01 9 31 1.2 24.1

OT-12-01 17 56 -2.1 23.8

OT-12-01 29 96 0.8 25.0

BA-09-01 55 180 0.5 23.9

BA-10-02 57 186 -2.4 24.7

62

Table 6

Carbon 14 Data Results

Footage Radiocarbon age

Lab ID Core ID (meters) (feet) BP Error

D-AMS 004776 BA-10-02 9 31 22,929 109

D-AMS 004151 OT-12-01 9 31 22,929 121

UGAMS 01900 KA-03-04 11 56 22,450 150

D-AMS 004152 OT-12-01 29 96 19,327 97

D-AMS 004148 BA-09-01 55 180 18,276 67

D-AMS 004152 BA-10-02 57 186 16,799 58

63

CHAPTER VI

DISCUSSION

Geotechnical analyses, grain size, textural classification, consistency, along

with glacial lithologies described in previous chapters, were used to identify the

stratigraphic framework, to interpret lithologic units and to correlate sediments of

glacial advances/retreat. Correlation of units was focused on the diamicton units

based on their stratigraphy and grain size distribution. Glacial deposits such as

diamicton serve as evidence of glacial advance/retreat, and are usually present as

nearly continuous layers of sediments. Analysis of these layers affords the ability to

accurately correlate these types of sediments across an area. The five cores analyzed;

BA-09-02, BA-10-02, KA-12-02, CA-11-01 and KA-13-01, each have between one

and four diamicton units.

Core Interpretations

Core BA-09-02 was drilled in landsystem 3. The area represents stagnation

and tunnel valleys in the area are assumed to have been formed by subglacial

meltwater (Kehew et al. 2012a). The core BA-09-02 contains two thick diamicton

units separated by silt/clay units. Ewald (2012) interprets these silt/clay units as

lacustrine sequences based on their thickness, lamination and texture. Diamicton in

this core consists of thick clay loam units, one near the surface (Unit A-1), and the

other close to the middle section (Unit A-2) just above a silty clay unit (Figure 19).

64

Figure 19. Matrix texture (<2.00 mm) of diamicton samples in BA-09-02. Red circles

represent upper diamicton (Unit A-1), orange circles represent middle diamicton

(Unit A-2). The lower diamicton samples have more silt and clay when compared to

the upper diamicton samples.

65

Figure 20. Matrix texture (<2.00 mm) of diamicton samples in BA-10-02. Red circles

represent upper diamicton (Unit B-1), orange circles represent middle diamicton

(Unit B-2), black circles represent lower diamicton (Unit B-3). The middle diamicton

samples have more sand than the upper and lower units. In the lower diamicton

samples, sand content decreases and clay content increase with depth.

66

Figure 21. Matrix texture (<2.00 mm) of diamicton samples in KA-12-02. Red circles

represent upper diamicton (Unit C-1). Samples in this unit are mainly sandy and silty,

with an increase in clay content in the upper and bottom sections.

67

Clay consistency in these diamictons varies from low plasticity in the upper and

bottom to medium plasticity in the middle section.

Cores BA-10-02 and KA-12-02 were drilled in landsystem 2. Laminated silts

and clays sediments in the area are assumed to have been deposited in a

glaciolacustrine environment (Ewald, 2012). Clay consistency in the diamictons from

this boring varies from slight to low plasticity. Core BA-10-02 contains three main

diamicton units and is separated by lacustrine sequences. The upper (Unit B-1) and

middle (Unit B-2) diamictons are mainly sandy loam units. The lower diamicton

(Unit B-3) is a very coarse sandy loam unit with high gravel content (Figure 20).

Core KA-12-02 contains one thick diamicton unit of about 13 meters between

silt/clay sediments probably deposited by meltwater during deglaciation. The

diamicton (Unit C-1) is a loam unit composed mostly of sand and silt (Figure 21).

Core KA-12-02 is located in an ice marginal zone; sediments in this area are mostly a

product of the stagnation and melting of the Saginaw lobe. Lacustrine sequences are

present above the diamicton unit and between -49 and -65 meters. The shale bedrock

is overlain by thick coarse sediments. Both cores BA-10-02 and KA-12-02 seem to

correlate in at least one diamicton unit.

Cores CA-11-01 and KA-13-01 were drilled in landsystem 1. The surficial

geology of the area consists of drumlins and outwash deposits. Diamictons in this

area are mostly sandy units, with a clay consistency ranging from slight in the first

-30 meters, to low/medium below the -40 meters. Core CA-11-01 contains four thick

68

Figure 22. Matrix texture (<2.00 mm) of diamicton samples in CA-11-01. Red circles

represent upper diamicton (Unit D-1), orange circles represent upper middle

diamicton (Unit D-2), black circles represent lower middle diamicton (Unit D-3),

green circles represent lower diamicton (Unit D-3). Samples from the upper and

middle diamictons are mainly sandy units. The lower diamicton samples have more

silt and clay than the upper units.

69

Figure 23. Matrix texture (<2.00 mm) of diamicton samples in KA-13-01. Red circles

represent upper diamicton (Unit E-1), orange circles represent middle diamicton (Unit

E-2). Diamicton samples in this core are mainly sandy and silty, with and average

clay content of 10%.

70

diamicton units separated by sand and gravel. Sand and gravel between diamictons

are poorly sorted, and are interpreted as outwash deposits. The first three diamicton

(Unit D-1, D-2, and D-3) are sandy loam units. The forth diamicton (Unit D-4) lies

above the bedrock and consists of a loam unit rich in silt (Figure 22). The bedrock is

siltstone, which explains the high silt content in the lowest diamicton unit. Core KA-

13-01 contains two diamicton unit separated mainly by gravel and sand. Both

diamictons are sandy units; the upper diamicton (Unit E-1) has a thickness of 11

meters, the lower diamicton (Unit E-2) has significantly more clay than the first one

and a thickness of 1.5 meters (Figure 23). Gravel followed by sand are the

predominant fractions in this core. Diamicton in drumlins were the product of

subglacial deposition and as the ice retreated outwash and other coarse sediments

were deposited along the area.

Landsystem Correlation across the Saginaw Lobe

Sediments in the uplands between landsystem 3, 2 and 1, consist mainly of

diamicton and lacustrine deposits. For this thesis sedimentary packages along the

south-central portion of the Lower Peninsula of Michigan have been tentatively

correlated in cross section A-A’ (Figure 25). Diamicton units indicate the presence of

at least one major and two minor advances/retreats of the Saginaw Lobe. Cores CA-

11-01 and KA-13-01 were collected from a drumlinized till plain across landsystem 1.

The bedrock elevation is shallow in this area, and decreases to the north and west of

the study area. Sediments in KA-13-01 vary from sandy diamicton, of which the

71

Figure 24. Matrix texture (<2.00 mm) of diamicton samples from cores: BA-09-02,

BA-10-02, KA-12-02, CA-11-01 and KA-13-01. Red circles represent upper

diamicton samples from depth between 0 to -31 meters; orange circles represent

lower diamicton samples from depth between -32 to -74 meters. The upper diamicton

samples have more sand when compared to the lower diamicton samples.

72

Figure 25. Cross Section A-A’: Proposed Correlation of Sediments. Correlated sedimentary packages in landsystem 1, 2 and 3. Glacial sediments were grouped in 3 different categories (Silt, Clay & Fine sand,

Sand&Gravel and Diamicton) for better interpretations. Solid gray lines the bedrock elevation. Sedimentary packages in the cross section indicate at least one major glacial retreat and two minor advances/retreats.

73

drumlins are formed, to gravel and some sand sequences. Glacial deposits become

finer close to core CA-11-01 (Figure 25). However, the area between CA-11-01 and

KA-13-01 is formed by outwash deposits; a fluctuation in the ice margin is the most

likely cause. Sediments tend to be coarsest close to KA-13-01 and finer near CA-11-

01. The ice lobe retreated from KA-13-01 leaving till and outwash deposit (coarse)

and paused 1 to 2 times before reaching the area near the Kalamazoo Valley. During

deglaciation, glacial deposits in this valley were eroded to or near the bedrock by a

downcutting event of high meltwater discharge that flowed through the area

(Kozlowski et al, 2005).

Sediments north of the Kalamazoo Valley consist of lacustrine (near core BA-

10-02) and outwash deposits (close to core KA-12-02), formed by stagnation and

downwasting of the ice lobe. North of the Kalamazoo Valley nearly continuous layers

of diamicton cross landsystem 2 and 3 (Figure 25). Glacial sediments in these two

areas are mostly lacustrine sequences, outwash and diamicton. Between 2 to 3

diamicton layers are present in this area, indicating at least one major glacial retreat

and two minor advances/retreats. Core BA-10-02 and KA-12-02 were drilled in

lansystem 2. Sedimentary packages observed around core KA-12-02 consist of a thick

layer of outwash deposit (sand) and diamicton. These sediments along with an

absence of lacustrine sequences point to a rapid melting in the ice lobe, leaving sand

and diamicton before reaching the area around core BA-10-02 where lacustrine

sequences began to reappear. Ewald (2012) explained that lacustrine sediments in the

area were the result of proglacial lake deposition, in which bedrock topography

74

played a major controlling factor. Lower bedrock elevations tend to impound most of

the lobe’s meltwater creating the right conditions for lacustrine sediments deposition.

Sedimentary packages across cores BA-09-02 and BA-10-02 evidence at least

three cyclical deposits of diamicton and lacustrine units, suggesting a series of

advances and retreats (Figure 25). Evidence provided by core BA-09-02 suggest that

at least two other cycles of advance and retreat took place within landsystem 3 after a

major retreat from landsystems 1 and 2. Final glacial events around the Thornapple

Valley include erosion by meltwater flow, probably from the Huron-Erie Lobe, which

eroded most of the upper sediments.

Interpretations and correlations made in this thesis related to the various

sedimentary packages across the Saginaw Lobe’s landsystems have been done using

the major stratigraphic units in the boreholes. Grain size distribution and sediment

stratigraphy were assumed to be the same as in their natural environment.

Additionally the 14

C method was used to date diamicton bulk organic carbon, to

identify with greater accuracy the cycles of advance and retreat across the ice lobe’s

landsystems. Unfortunately the method has proven ineffective in these glacial soils,

resulting in dates evidencing no correlation with each other or other previous

radiocarbon data (Table 5). This study suggests other geotechnical methods which

could help to identify and even determine diamicton genesis (subglacial or

supraglacial) like unit weight, vertical stress, compressibility and shear strength.

These types of analyses are beyond the scope of this project, but could be useful in

future studies.

75

CHAPTER VII

CONCLUSIONS

Five cores were analyzed to delineate the Saginaw Lobe subsurface drift

stratigraphy in the south-central portion of the Lower Michigan Peninsula. These

borings were selected according to their diamicton (till) content. Sedimentary

packages in cores BA-09-02, BA-10-02, KA-12-02 were mainly composed of

diamicton, clay and silt, while cores CA-11-01 and KA-13-01were mostly composed

of diamicton, sand and gravel. Diamicton units in these cores were correlated across

the area using water well logs, surficial geology maps and bedrock topography.

This study brings new information about the environment in which glacial

sediments were deposited and their relation with the Saginaw Lobe‘s advances and

retreats. The analyses indicate that sediments located between the Thornapple Valley

and Kalamazoo Moraine consists mainly of cyclical deposits of clayey diamicton and

lacustrine sequences, and south of the Kalamazoo Moraine by sandy diamicton and

very coarse outwash deposits. These glacial deposits serve as evidence of at least

three main glacial events: one major cycle of advances/retreats followed by two

minor cycles of advance/retreat. Bedrock topography also played an active role by

controlling the advance of the Saginaw lobe.

Bedrock topography delineated in this study also shows a correlation between

bedrock elevation and the distribution between coarse outwash deposits and lacustrine

76

sequences. Lower bedrock elevations tend to impound most of the lobe’s meltwater

creating the right conditions for lacustrine sediment deposition.

77

APPENDIX A

Particle Size Analysis Results

78

Tota

l W

eig

ht

Sam

ple

ID

5 (φ

= -

2)10

(φ

= -

1)18

(φ

= 0

)35

(φ

= 1

)60

(φ

= 2

)12

0 (φ

= 3

)23

0 (φ

= 4

)Si

lt (

φ ≥

5)

Cla

y (φ

≥ 5

)(G

ram

s)

1 (A

)-2

.50

-4.5

00.

730.

631.

537.

4065

.89

83.6

546

.58

126.

6864

.98

398.

07

2 (B

)0.

00-2

.50

0.00

0.11

0.60

5.62

45.9

764

.83

52.8

116

9.04

59.9

539

8.93

3 (C

)-5

.25

-7.0

04.

824.

377.

1816

.79

67.2

291

.23

55.0

111

7.78

34.8

939

9.29

4 (D

)-7

.00

-11.

000.

370.

692.

5010

.28

58.9

281

.64

48.9

512

7.87

69.1

340

0.35

5 (E

)-1

1.75

-12.

2526

7.26

35.7

024

.24

32.9

618

.21

7.00

5.15

7.35

2.88

400.

75

6 (F

)-1

2.25

-14.

0013

6.46

53.8

541

.75

78.7

469

.74

6.08

4.53

8.13

1.59

400.

87

7 (G

)-1

1.00

-11.

7511

3.15

38.1

334

.69

60.9

492

.51

24.5

412

.98

18.7

54.

8040

0.49

8 (H

)-1

4.00

-15.

0013

5.39

68.4

471

.93

72.6

337

.51

4.31

3.04

5.71

1.13

400.

09

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46 (

TT)

-137

.50

-142

.50

0.59

0.80

0.93

1.48

5.89

8.57

5.93

24.2

043

.08

32.7

310

0.00

47 (

UU

)-1

42.5

0-1

45.5

00.

700.

390.

711.

947.

4213

.35

8.50

33.0

137

.60

29.3

810

0.00

48 (

VV

)-1

45.5

0-1

49.4

00.

900.

320.

430.

844.

0412

.97

12.4

331

.93

43.3

524

.73

100.

00

49 (

WW

)-1

49.4

0-1

50.5

00.

000.

000.

010.

4960

.14

37.4

80.

9799

.09

0.73

0.18

100.

00

50 (

XX)

-150

.50

-155

.00

0.38

0.85

0.70

1.41

5.76

10.0

86.

6525

.84

44.6

629

.50

100.

00

51 (

YY)

-155

.00

-157

.50

0.00

0.00

0.00

0.00

0.01

0.06

0.18

0.25

59.6

340

.12

100.

00

52 (

ZZ)

-157

.50

-162

.50

0.00

0.00

0.00

0.00

0.01

0.06

0.67

0.74

50.6

448

.62

100.

00

53 (

AA

A)

-162

.50

-167

.50

0.00

0.00

0.00

0.00

0.01

0.04

0.51

0.57

51.8

947

.54

100.

00

54 (

BB

B)

-167

.50

-172

.50

0.00

0.00

0.00

0.00

0.00

0.04

0.71

0.74

44.3

954

.87

100.

00

55 (

CCC)

-172

.50

-178

.00

0.00

0.00

0.00

0.00

0.01

0.08

0.89

0.97

50.2

948

.74

100.

00

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

BA

-09-

02 S

ampl

e W

eigh

t Pe

rcen

tsG

rave

l &

Sa

nd

Tota

l (%

)

82

Sample ID % Gravel % Sand % Si l t % Clay % Tota l % Sand % Si l t % Clay

1 (A) -2.50 -4.50 0.34 51.51 31.82 16.32 100.00 51.69 31.93 16.38

2 (B) 0.00 -2.50 0.03 42.57 42.37 15.03 100.00 42.58 42.38 15.03

3 (C) -5.25 -7.00 2.30 59.46 29.50 8.74 100.00 60.86 30.19 8.94

4 (D) -7.00 -11.00 0.26 50.53 31.94 17.27 100.00 50.66 32.03 17.31

5 (E) -11.75 -12.25 75.60 21.85 1.83 0.72 100.00 89.54 7.51 2.95

6 (F) -12.25 -14.00 47.47 50.10 2.03 0.40 100.00 95.38 3.86 0.76

7 (G) -11.00 -11.75 37.77 56.35 4.68 1.20 100.00 90.55 7.52 1.93

8 (H) -14.00 -15.00 50.95 47.34 1.43 0.28 100.00 96.51 2.91 0.58

9 (I) -15.00 -16.00 31.42 67.50 0.85 0.23 100.00 98.43 1.24 0.34

10 (J) -16.00 -18.00 52.81 46.59 0.47 0.13 100.00 98.72 1.01 0.28

11 (K) -18.00 -20.00 22.13 77.13 0.58 0.16 100.00 99.05 0.75 0.20

12 (L) -20.00 -21.00 1.95 97.78 0.22 0.06 100.00 99.72 0.22 0.06

13 (M) -21.00 -22.00 0.14 99.40 0.38 0.08 100.00 99.54 0.39 0.08

14 (N) -22.00 -23.00 0.06 98.83 0.99 0.13 100.00 98.89 0.99 0.13

15 (O) -23.00 -24.00 0.00 1.80 85.37 12.83 100.00 1.80 85.37 12.83

16 (P) -24.00 -28.00 0.00 0.56 59.61 39.83 100.00 0.56 59.61 39.83

17 (Q) -28.00 -33.00 0.00 1.14 58.98 39.88 100.00 1.14 58.98 39.88

18 (R) -33.00 -36.00 0.00 1.24 62.55 36.20 100.00 1.24 62.55 36.20

19 (S) -36.00 -36.50 9.52 85.93 3.67 0.88 100.00 94.97 4.06 0.97

20 (T) -38.50 -41.00 27.76 71.47 0.63 0.14 100.00 98.94 0.87 0.19

21 (U) -41.00 -43.00 80.59 18.20 1.06 0.15 100.00 93.79 5.45 0.76

22 (V) -43.00 -45.00 34.73 64.84 0.34 0.09 100.00 99.34 0.52 0.14

23 (W) -45.75 -46.25 11.89 46.46 32.95 8.70 100.00 52.73 37.39 9.88

24 (X) -45.00 -45.75 17.87 32.50 31.98 17.65 100.00 39.57 38.94 21.49

25 (Y) -46.25 -47.20 23.25 62.49 10.60 3.66 100.00 81.43 13.81 4.76

26 (Z) -36.50 -38.12 0.05 7.19 66.40 26.35 100.00 7.20 66.44 26.37

27 (AA) -47.20 -50.00 44.47 49.64 5.33 0.56 100.00 89.38 9.61 1.01

28 (BB) -50.00 -53.50 20.86 68.77 9.53 0.84 100.00 86.90 12.04 1.06

29 (CC) -53.50 -57.50 3.15 31.43 39.61 25.81 100.00 32.45 40.90 26.65

30 (DD) -57.50 -62.50 1.74 34.21 39.66 24.39 100.00 34.81 40.36 24.82

31 (EE) -62.50 -67.50 3.84 39.84 36.20 20.11 100.00 41.43 37.65 20.92

32 (FF) -67.50 -73.00 6.43 27.80 39.71 26.07 100.00 29.71 42.44 27.86

33 (GG) -73.00 -76.00 1.68 22.75 45.71 29.86 100.00 23.14 46.49 30.37

34 (HH) -76.00 -82.00 0.00 0.40 80.74 18.87 100.00 0.40 80.74 18.87

35 (II) -82.00 -87.50 0.00 0.99 76.32 22.69 100.00 0.99 76.32 22.69

36 (JJ) -87.50 -92.50 0.00 1.11 63.28 35.61 100.00 1.11 63.28 35.61

37 (KK) -92.50 -97.50 0.00 0.49 59.65 39.86 100.00 0.49 59.65 39.86

38 (LL) -97.50 -102.50 0.18 2.00 53.63 44.19 100.00 2.00 53.73 44.27

39 (MM) -102.50 -108.00 0.05 2.71 61.49 35.75 100.00 2.71 61.52 35.77

40 (NN) -108.00 -114.00 0.10 7.81 53.54 38.55 100.00 7.82 53.60 38.59

41 (OO) -114.00 -117.50 1.70 20.44 46.15 31.71 100.00 20.79 46.95 32.26

42 (PP) -117.50 -122.50 3.55 32.85 36.31 27.29 100.00 34.06 37.64 28.29

43 (QQ) -122.50 -127.50 3.35 28.94 38.25 29.46 100.00 29.94 39.58 30.48

44 (RR) -127.50 -132.50 2.54 22.15 49.25 26.06 100.00 22.72 50.54 26.74

45 (SS) -132.50 -137.50 2.26 26.75 45.94 25.05 100.00 27.36 47.00 25.63

46 (TT) -137.50 -142.50 1.39 22.81 43.08 32.73 100.00 23.13 43.68 33.19

47 (UU) -142.50 -145.50 1.09 31.93 37.60 29.38 100.00 32.28 38.02 29.71

48 (VV) -145.50 -149.40 1.22 30.71 43.35 24.73 100.00 31.09 43.88 25.03

49 (WW) -149.40 -150.50 0.00 99.09 0.73 0.18 100.00 99.09 0.73 0.18

50 (XX) -150.50 -155.00 1.23 24.61 44.66 29.50 100.00 24.91 45.22 29.87

51 (YY) -155.00 -157.50 0.00 0.25 59.63 40.12 100.00 0.25 59.63 40.12

52 (ZZ) -157.50 -162.50 0.00 0.74 50.64 48.62 100.00 0.74 50.64 48.62

53 (AAA) -162.50 -167.50 0.00 0.57 51.89 47.54 100.00 0.57 51.89 47.54

54 (BBB) -167.50 -172.50 0.00 0.74 44.39 54.87 100.00 0.74 44.39 54.87

55 (CCC) -172.50 -178.00 0.00 0.97 50.29 48.74 100.00 0.97 50.29 48.74

Depth (feet from surface)

Normalized SampleBA-09-02 Sample Particle Size Distribution

83

Tota

l W

eig

ht

Sam

ple

ID

5 (

φ =

-2

)1

0 (

φ =

-1

)1

8 (

φ =

0)

35

(φ

= 1

)6

0 (

φ =

2)

12

0 (

φ =

3)

23

0 (

φ =

4)

Silt

(φ

≥ 5

)C

lay

(φ ≥

5)

(Gra

ms)

1 (

A)

-1.5

0-2

.50

66

.84

38

.28

37

.53

42

.05

88

.02

70

.23

28

.64

21

.73

8.2

34

01

.55

2 (

B)

-2.5

0-6

.70

0.4

61

.21

2.3

15

.01

20

.00

25

.09

21

.45

18

2.6

01

55

.04

41

3.1

7

3 (

C)

-6.7

0-8

.70

2.8

90

.79

0.7

81

.84

5.5

11

5.2

18

4.4

52

64

.88

73

.14

44

9.4

9

4 (

D)

-8.7

0-1

0.0

00

.00

4.7

86

.82

4.0

76

9.1

21

34

.95

62

.19

12

6.6

92

5.8

04

34

.42

5 (

E)-1

0.0

0-1

4.1

06

.90

12

.49

10

.69

12

.93

14

0.0

92

11

.67

47

.44

14

.32

1.8

14

58

.34

6 (

F)-1

4.1

0-1

5.5

06

.06

3.5

93

.13

3.8

61

1.2

51

4.5

19

.50

60

.52

46

.55

15

8.9

7

7 (

G)

-15

.50

-16

.50

57

.85

57

.41

45

.85

48

.67

89

.80

83

.14

16

.02

4.5

11

.05

40

4.3

0

8 (

H)

-16

.50

-17

.50

10

0.4

17

1.3

96

3.6

25

9.5

09

2.7

35

2.5

41

5.0

19

.88

3.8

24

68

.90

9 (

I)-1

7.5

0-1

9.5

03

2.9

01

1.5

51

2.9

41

7.6

94

3.1

93

9.6

11

8.6

09

1.8

38

1.9

63

50

.27

10

(J)

-19

.50

-21

.20

64

.49

18

.28

24

.06

46

.41

12

1.8

48

1.9

12

7.1

41

5.4

12

.81

40

2.3

5

11

(K

)-2

1.2

0-2

5.2

02

4.4

39

.76

9.6

21

5.0

14

8.8

45

9.8

83

3.7

11

72

.07

74

.48

44

7.8

0

12

(L)

-25

.20

-26

.00

0.0

60

.05

0.4

63

.09

10

.86

98

.46

16

8.8

11

93

.29

10

.56

48

5.6

4

13

(M

)-2

6.0

0-2

6.5

05

7.1

92

3.6

92

8.4

66

1.7

61

24

.38

70

.15

24

.58

9.5

91

.11

40

0.9

1

14

(N

)-2

7.1

0-3

0.0

01

6.7

48

.70

9.8

21

6.6

45

7.7

57

1.3

73

9.2

81

67

.29

71

.28

45

8.8

7

15

(O

)-3

0.0

0-3

5.0

09

.14

9.4

39

.65

17

.05

63

.20

81

.01

42

.73

14

3.7

97

4.5

94

50

.59

16

(P

)-3

5.0

0-4

0.0

01

8.5

89

.63

8.9

81

6.5

56

4.0

87

9.4

35

0.2

41

69

.02

32

.28

44

8.7

9

17

(Q

)-4

0.0

0-4

3.6

01

30

.23

14

.71

13

.73

36

.12

11

0.3

51

05

.06

43

.49

40

.39

6.3

05

00

.38

18

(R

)-4

3.6

0-4

9.5

00

.44

0.8

01

.07

5.9

13

2.1

26

8.0

61

31

.26

17

8.6

63

1.0

54

49

.37

19

(S)

-49

.50

-53

.00

0.0

01

.57

6.8

52

5.2

31

36

.56

16

5.5

44

9.1

41

4.8

30

.86

40

0.5

8

20

(T)

-53

.00

-56

.50

29

.02

23

.10

34

.10

57

.84

13

6.9

69

8.0

41

6.8

04

.25

0.4

04

00

.51

21

(U

)-5

6.5

0-5

9.1

00

.31

0.4

30

.41

0.6

52

.12

19

.78

11

9.0

22

74

.49

15

.39

43

2.6

0

22

(V

)-5

9.1

0-6

7.6

00

.15

1.2

04

.46

22

.65

10

0.7

41

81

.59

63

.85

24

.42

1.2

94

00

.35

23

(W

)-6

7.6

0-6

9.0

00

.00

0.0

80

.30

0.3

70

.81

1.1

41

.28

17

8.9

16

8.7

42

51

.63

24

(X

)-6

9.5

0-7

0.5

00

.00

0.0

30

.00

0.0

60

.38

1.5

72

6.2

11

40

.25

11

.68

18

0.1

8

25

(Y)

-70

.50

-75

.00

3.5

13

.72

6.6

42

9.8

72

50

.29

10

0.1

98

.13

2.0

20

.13

40

4.5

0

26

(Z)

-69

.00

-69

.50

0.0

00

0.2

11

.92

47

.11

53

.69

78

.99

45

.53

2.2

83

29

.72

27

(A

A)

-75

.00

-77

.50

35

.58

16

.81

9.7

92

7.9

12

22

.93

83

.47

3.1

31

.07

0.0

94

00

.78

28

(B

B)

-77

.50

-78

.50

0.0

01

.16

2.1

67

.02

85

.87

24

9.0

34

9.1

86

.07

0.1

84

00

.67

29

(C

C)

-78

.50

-80

.00

37

.84

72

.26

84

.26

10

0.5

81

.42

18

.75

4.0

01

.28

0.1

94

00

.50

30

(D

D)

-80

.00

-81

.00

1.4

31

1.3

35

7.4

61

19

.57

13

8.9

55

8.4

68

.93

.84

0.4

24

00

.36

31

(EE

)-8

1.0

0-8

2.0

02

44

.25

45

.69

24

.64

22

.98

48

.15

40

.15

13

.14

10

.16

1.2

54

50

.41

32

(FF

)-8

2.0

0-9

0.0

06

2.5

01

2.9

61

2.5

52

2.5

98

9.6

81

02

.14

51

.61

18

.34

19

.81

49

2.1

7

33

(G

G)

-90

.00

-98

.40

31

.51

12

.07

14

.34

23

.54

84

.86

95

.23

47

.53

10

6.9

13

0.1

84

46

.17

34

(H

H)

-98

.40

-10

0.0

04

8.3

92

0.1

12

4.9

49

.67

17

1.0

56

3.8

41

1.8

79

.05

1.4

94

00

.37

35

(II

)-1

00

.00

-10

2.7

01

51

.66

39

.03

33

.51

59

.54

14

9.5

10

0.2

14

1.5

15

5.4

19

.57

63

9.9

4

De

pth

(fe

et

fro

m s

urf

ace

)

Pa

n (

ph

i V

alu

e)

Sie

ve N

um

be

r (p

hi

Va

lue

)B

A-1

0-0

2 S

amp

le M

asse

s

84

Tota

l W

eig

ht

Sam

ple

ID

5 (

φ =

-2

)1

0 (

φ =

-1

)1

8 (

φ =

0)

35

(φ

= 1

)6

0 (

φ =

2)

12

0 (

φ =

3)

23

0 (

φ =

4)

Silt

(φ

≥ 5

)C

lay

(φ ≥

5)

(Gra

ms)

36

(JJ

)-1

02

.70

-10

4.0

01

28

.51

17

.14

17

.94

33

.61

11

.87

99

.13

8.0

78

3.6

92

7.4

15

57

.33

37

(K

K)

-10

4.0

0-1

05

.00

5.9

87

.87

11

.82

54

.54

23

9.5

66

7.8

96

.48

5.3

90

.83

40

0.3

6

38

(LL

)-1

05

.00

-10

7.0

01

8.4

91

4.1

12

4.3

46

7.6

12

08

.42

58

.53

4.9

23

.52

0.6

54

00

.59

39

(M

M)

-10

7.0

0-1

08

.00

5.8

10

.51

2.0

18

.52

99

.01

22

8.0

24

1.3

31

3.6

41

.49

40

0.3

4

40

(N

N)

-10

8.0

0-1

09

.50

71

.01

44

.95

48

.08

67

.28

11

7.2

13

1.4

28

.67

10

.65

1.3

24

00

.59

41

(O

O)

-10

9.5

0-1

11

.80

13

.29

18

.62

32

.93

97

.83

19

4.8

12

7.8

54

.47

9.1

01

.72

40

0.6

2

42

(P

P)

-11

1.8

0-1

14

.50

0.0

00

0.0

30

.23

43

.72

30

2.7

84

5.4

28

.37

0.0

04

00

.55

43

(Q

Q)

-11

4.5

0-1

19

.00

0.0

00

00

.75

10

.35

17

0.9

11

70

.42

35

.18

12

.67

40

0.2

8

44

(R

R)

-11

9.0

0-1

21

.00

0.0

00

0.0

40

.25

23

.09

15

4.6

78

.49

13

3.7

35

4.2

94

44

.49

45

(SS

)-1

21

.00

-13

1.7

00

.00

00

00

.37

10

5.5

20

1.7

71

03

.74

7.4

24

18

.80

46

(TT

)-1

31

.70

-13

2.6

00

.00

00

0.1

11

.01

11

.03

89

.51

28

4.0

35

3.6

34

39

.32

47

(U

U)

-13

2.6

0-1

36

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0.0

00

00

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0.1

11

9.5

92

01

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12

7.2

56

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35

5.1

5

48

(V

V)

-13

6.0

0-1

40

.00

0.0

00

00

.04

0.1

34

0.0

52

15

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14

9.2

78

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41

3.1

6

49

(W

W)

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46

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0.0

00

00

.02

0.5

32

9.2

91

88

.65

16

0.6

91

2.8

23

92

.00

50

(X

X)

-14

6.4

0-1

49

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0.0

00

00

.02

0.1

51

5.3

91

43

.89

21

8.2

52

3.8

54

01

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51

(YY

)-1

49

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9.0

00

.00

00

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0.1

81

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12

.53

22

5.0

32

04

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17

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46

0.7

1

52

(ZZ

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59

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0.0

00

.00

00

0.0

30

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1.6

63

3.8

92

77

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47

.52

36

1.3

6

53

(A

AA

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60

.00

-16

7.0

00

.00

00

0.0

10

.05

1.4

41

25

.17

27

4.6

41

2.8

44

14

.15

54

(B

BB

)-1

67

.00

-17

7.3

00

.00

00

00

.19

27

.86

15

8.5

82

08

.07

17

.07

41

1.7

7

55

(C

CC

)-1

77

.30

-18

4.0

02

39

.09

22

.79

18

.52

22

.04

56

.13

71

.35

37

.32

11

3.4

56

4.0

26

44

.71

56

(D

DD

)-1

84

.00

-19

0.0

02

54

.68

22

.63

25

.77

26

.95

0.2

48

2.2

91

.14

13

9.0

02

2.6

97

15

.25

57

(EE

E)-1

90

.00

-19

2.2

03

45

.17

77

.62

56

.58

41

.55

39

.11

18

.49

10

.44

16

.23

3.2

46

08

.43

58

(FF

F)-1

92

.20

-20

0.0

05

.40

2.5

53

.26

10

.05

21

.22

4.6

42

5.7

31

79

.15

11

6.9

93

88

.97

59

(G

GG

)-2

00

.00

-20

5.2

00

.00

0.0

60

.06

0.1

20

.43

0.6

11

0.1

38

1.2

25

7.6

14

50

.21

60

(H

HH

)-2

05

.20

-20

8.0

04

.83

2.9

27

.78

24

.62

41

.62

40

.94

29

.31

17

3.5

19

9.4

44

24

.97

61

(II

I)-2

08

.00

-21

1.0

01

.14

1.7

32

.56

10

.21

27

.04

31

.68

26

.08

21

5.2

71

08

.55

42

4.2

6

62

(JJ

J)-2

11

.00

-21

5.0

07

2.9

52

4.1

32

1.0

52

4.6

48

2.6

21

25

.26

50

.79

12

1.5

62

4.9

95

47

.99

63

(K

KK

)-2

20

.00

-22

2.8

00

.19

0.3

60

.23

2.2

25

1.7

15

2.5

25

3.0

41

81

.26

90

.76

43

2.2

9

64

(LL

L)-2

22

.80

-22

5.0

02

1.6

19

.92

8.8

11

4.7

59

.65

11

1.3

26

3.9

21

38

.27

17

.80

44

6.0

0

65

(M

MM

)-2

25

.00

-22

7.0

01

2.7

62

65

2.6

37

1.2

11

1.2

41

00

.07

14

.34

5.8

50

.83

39

4.9

2

66

(N

NN

)-2

27

.00

-23

0.0

00

.00

0.1

20

.13

0.6

51

12

.94

24

7.9

62

8.9

8.7

50

.76

40

0.2

1

67

(O

OO

)-2

30

-23

3.3

00

0.0

50

.31

10

.56

24

2.2

83

5.7

31

0.3

70

.94

40

0.2

3

68

(P

PP

)-2

33

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37

14

51

9.6

11

4.0

91

6.1

75

0.5

97

6.3

63

8.9

31

15

.39

49

.21

52

5.3

5

69

(Q

QQ

)-2

37

-24

06

6.9

51

.21

.78

3.2

37

.51

5.7

95

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22

4.0

51

81

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49

7.4

9

De

pth

(fe

et

fro

m s

urf

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Pa

n (

ph

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alu

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Sie

ve N

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be

r (p

hi

Va

lue

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le M

asse

s

85

Sam

ple

ID

5 (

φ =

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φ =

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φ =

0)

35

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φ =

2)

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φ =

3)

23

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φ =

4)

Silt

(φ

≥ 5

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lay

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Sam

ple

To

tal

(%)

1 (

A)

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16

.65

9.5

39

.35

10

.47

21

.92

17

.49

7.1

39

2.5

45

.41

2.0

51

00

.00

2 (

B)

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0-6

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0.1

10

.29

0.5

61

.21

4.8

46

.07

5.1

91

8.2

84

4.2

03

7.5

21

00

.00

3 (

C)

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0-8

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0.6

40

.18

0.1

70

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1.2

33

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18

.79

24

.80

58

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16

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10

0.0

0

4 (

D)

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00

.00

1.1

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0.9

41

5.9

13

1.0

61

4.3

26

4.9

02

9.1

65

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10

0.0

0

5 (

E)-1

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01

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2.7

32

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2.8

23

0.5

64

6.1

81

0.3

59

6.4

83

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0.3

91

00

.00

6 (

F)-1

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03

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2.2

61

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2.4

37

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35

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32

.65

38

.07

29

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10

0.0

0

7 (

G)

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-16

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14

.31

14

.20

11

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12

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22

.21

20

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3.9

69

8.6

21

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0.2

61

00

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8 (

H)

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-17

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21

.41

15

.22

13

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12

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19

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11

.20

3.2

09

7.0

82

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0.8

21

00

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9 (

I)-1

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9.5

09

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3.3

03

.69

5.0

51

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31

1.3

15

.31

50

.38

26

.22

23

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10

0.0

0

10

(J)

-19

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-21

.20

16

.03

4.5

45

.98

11

.53

30

.28

20

.36

6.7

59

5.4

73

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0.7

01

00

.00

11

(K

)-2

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0-2

5.2

05

.46

2.1

82

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3.3

51

0.9

11

3.3

77

.53

44

.94

38

.42

16

.63

10

0.0

0

12

(L)

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-26

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0.0

10

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0.0

90

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2.2

42

0.2

73

4.7

65

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23

9.8

02

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10

0.0

0

13

(M

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6.5

01

4.2

75

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7.1

01

5.4

03

1.0

21

7.5

06

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97

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2.3

90

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10

0.0

0

14

(N

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0.0

03

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1.9

02

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3.6

31

2.5

91

5.5

58

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48

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36

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15

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10

0.0

0

15

(O

)-3

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02

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2.0

92

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3.7

81

4.0

31

7.9

89

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51

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31

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16

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10

0.0

0

16

(P

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04

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2.1

52

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3.6

91

4.2

81

7.7

01

1.1

95

5.1

53

7.6

67

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10

0.0

0

17

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)-4

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02

6.0

32

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2.7

47

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22

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21

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8.6

99

0.6

78

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1.2

61

00

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18

(R

)-4

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9.5

00

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0.1

80

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1.3

27

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15

.15

29

.21

53

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39

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6.9

11

00

.00

19

(S)

-49

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-53

.00

0.0

00

.39

1.7

16

.30

34

.09

41

.33

12

.27

96

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3.7

00

.21

10

0.0

0

20

(T)

-53

.00

-56

.50

7.2

55

.77

8.5

11

4.4

43

4.2

02

4.4

84

.19

98

.84

1.0

60

.10

10

0.0

0

21

(U

)-5

6.5

0-5

9.1

00

.07

0.1

00

.09

0.1

50

.49

4.5

72

7.5

13

2.9

96

3.4

53

.56

10

0.0

0

22

(V

)-5

9.1

0-6

7.6

00

.04

0.3

01

.11

5.6

62

5.1

64

5.3

61

5.9

59

3.5

86

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0.3

21

00

.00

23

(W

)-6

7.6

0-6

9.0

00

.00

0.0

30

.12

0.1

50

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0.4

50

.51

1.5

87

1.1

02

7.3

21

00

.00

24

(X

)-6

9.5

0-7

0.5

00

.00

0.0

20

.00

0.0

30

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0.8

71

4.5

51

5.6

87

7.8

46

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10

0.0

0

25

(Y)

-70

.50

-75

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0.8

70

.92

1.6

47

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61

.88

24

.77

2.0

19

9.4

70

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0.0

31

00

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26

(Z)

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-69

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0.0

00

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0.0

60

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14

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46

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23

.96

85

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13

.81

0.6

91

00

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27

(A

A)

-75

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-77

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8.8

84

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2.4

46

.96

55

.62

20

.83

0.7

89

9.7

10

.27

0.0

21

00

.00

28

(B

B)

-77

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-78

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0.0

00

.29

0.5

41

.75

21

.43

62

.15

12

.27

98

.44

1.5

10

.04

10

0.0

0

29

(C

C)

-78

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-80

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9.4

51

8.0

42

1.0

42

5.0

92

0.3

34

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1.0

09

9.6

30

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0.0

51

00

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30

(D

D)

-80

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-81

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0.3

62

.83

14

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29

.87

34

.71

14

.60

2.2

29

8.9

40

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0.1

01

00

.00

31

(EE

)-8

1.0

0-8

2.0

05

4.2

31

0.1

45

.47

5.1

01

0.6

98

.91

2.9

29

7.4

72

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0.2

81

00

.00

32

(FF

)-8

2.0

0-9

0.0

01

2.7

02

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2.5

54

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18

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20

.75

10

.48

71

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24

.04

4.0

21

00

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33

(G

G)

-90

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-98

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7.0

62

.71

3.2

15

.28

19

.02

21

.34

10

.65

69

.27

23

.96

6.7

61

00

.00

34

(H

H)

-98

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0.0

01

2.0

95

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6.2

21

2.4

14

2.7

21

5.9

52

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97

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2.2

60

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10

0.0

0

35

(II

)-1

00

.00

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2.7

02

3.7

06

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5.2

49

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23

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15

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6.4

98

9.8

58

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1.4

91

00

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De

pth

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et

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m s

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n (

ph

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Sam

ple

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(φ

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23

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Silt

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Sam

ple

To

tal

(%)

36

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02

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63

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3.2

26

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20

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17

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6.8

38

0.0

71

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24

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10

0.0

0

37

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K)

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05

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1.4

91

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2.9

51

3.6

25

9.8

41

6.9

61

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50

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10

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0

38

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26

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16

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52

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14

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39

8.9

60

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0.1

61

00

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39

(M

M)

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08

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1.4

50

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0.5

02

.13

24

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56

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10

.32

96

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3.4

10

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10

0.0

0

40

(N

N)

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0-1

09

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17

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11

.22

12

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16

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29

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7.8

42

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97

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2.6

60

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10

0.0

0

41

(O

O)

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9.5

0-1

11

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3.3

24

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8.2

22

4.4

24

8.6

36

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1.1

29

7.3

02

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0.4

31

00

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42

(P

P)

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0-1

14

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0.0

00

.00

0.0

10

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10

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75

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11

.34

97

.91

2.0

90

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10

0.0

0

43

(Q

Q)

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4.5

0-1

19

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0.0

00

.00

0.0

00

.19

2.5

94

2.7

04

2.5

88

8.0

58

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3.1

71

00

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44

(R

R)

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9.0

0-1

21

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0.0

00

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0.0

10

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5.1

93

4.7

81

7.6

65

7.7

03

0.0

91

2.2

11

00

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45

(SS

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21

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1.7

00

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0.0

00

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0.0

00

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25

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48

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73

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24

.77

1.7

71

00

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46

(TT

)-1

31

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-13

2.6

00

.00

0.0

00

.00

0.0

30

.23

2.5

12

0.3

72

3.1

46

4.6

51

2.2

11

00

.00

47

(U

U)

-13

2.6

0-1

36

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0.0

00

.00

0.0

00

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0.0

35

.52

56

.70

62

.25

35

.83

1.9

21

00

.00

48

(V

V)

-13

6.0

0-1

40

.00

0.0

00

.00

0.0

00

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0.0

39

.69

52

.05

61

.79

36

.13

2.0

81

00

.00

49

(W

W)

-14

0.0

0-1

46

.40

0.0

00

.00

0.0

00

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0.1

47

.47

48

.13

55

.74

40

.99

3.2

71

00

.00

50

(X

X)

-14

6.4

0-1

49

.20

0.0

00

.00

0.0

00

.00

0.0

43

.83

35

.83

39

.71

54

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5.9

41

00

.00

51

(YY

)-1

49

.20

-15

9.0

00

.00

0.0

00

.00

0.0

40

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2.7

24

8.8

45

1.8

44

4.3

23

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10

0.0

0

52

(ZZ

)-1

59

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-16

0.0

00

.00

0.0

00

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0.0

10

.24

0.4

69

.38

10

.09

76

.76

13

.15

10

0.0

0

53

(A

AA

)-1

60

.00

-16

7.0

00

.00

0.0

00

.00

0.0

00

.01

0.3

53

0.2

23

0.5

96

6.3

13

.10

10

0.0

0

54

(B

BB

)-1

67

.00

-17

7.3

00

.00

0.0

00

.00

0.0

00

.05

6.7

73

8.5

14

5.3

25

0.5

34

.15

10

0.0

0

55

(C

CC

)-1

77

.30

-18

4.0

03

7.0

83

.53

2.8

73

.42

8.7

11

1.0

75

.79

72

.47

17

.60

9.9

31

00

.00

56

(D

DD

)-1

84

.00

-19

0.0

03

5.6

13

.16

3.6

03

.76

7.0

21

1.4

91

2.7

47

7.3

91

9.4

33

.17

10

0.0

0

57

(EE

E)-1

90

.00

-19

2.2

05

6.7

31

2.7

69

.30

6.8

36

.43

3.0

41

.72

96

.80

2.6

70

.53

10

0.0

0

58

(FF

F)-1

92

.20

-20

0.0

01

.39

0.6

60

.84

2.5

85

.45

6.3

36

.61

23

.87

46

.06

30

.08

10

0.0

0

59

(G

GG

)-2

00

.00

-20

5.2

00

.00

0.0

10

.01

0.0

30

.10

0.1

42

.24

2.5

38

4.6

81

2.8

01

00

.00

60

(H

HH

)-2

05

.20

-20

8.0

01

.14

0.6

91

.83

5.7

99

.79

9.6

36

.90

35

.77

40

.83

23

.40

10

0.0

0

61

(II

I)-2

08

.00

-21

1.0

00

.27

0.4

10

.60

2.4

16

.37

7.4

76

.15

23

.67

50

.74

25

.59

10

0.0

0

62

(JJ

J)-2

11

.00

-21

5.0

01

3.3

14

.40

3.8

44

.50

15

.08

22

.86

9.2

77

3.2

62

2.1

84

.56

10

0.0

0

63

(K

KK

)-2

20

.00

-22

2.8

00

.04

0.0

80

.05

0.5

11

1.9

61

2.1

51

2.2

73

7.0

74

1.9

32

1.0

01

00

.00

64

(LL

L)-2

22

.80

-22

5.0

04

.85

2.2

21

.98

3.3

01

3.3

72

4.9

61

4.3

36

5.0

13

1.0

03

.99

10

0.0

0

65

(M

MM

)-2

25

.00

-22

7.0

03

.23

6.5

81

3.3

31

8.0

32

8.1

72

5.3

43

.63

98

.31

1.4

80

.21

10

0.0

0

66

(N

NN

)-2

27

.00

-23

0.0

00

.00

0.0

30

.03

0.1

62

8.2

26

1.9

67

.22

97

.62

2.1

90

.19

10

0.0

0

67

(O

OO

)-2

30

-23

3.3

0.0

00

.00

0.0

10

.07

27

.62

60

.54

8.9

39

7.1

72

.59

0.2

31

00

.00

68

(P

PP

)-2

33

.3-2

37

27

.60

3.7

32

.68

3.0

89

.63

14

.54

7.4

16

8.6

72

1.9

69

.37

10

0.0

0

69

(Q

QQ

)-2

37

-24

01

3.4

60

.24

0.3

60

.65

1.5

11

.16

1.1

31

8.5

14

5.0

43

6.4

51

00

.00

De

pth

(fe

et

fro

m s

urf

ace

)

Pa

n (

ph

i V

alu

e)

Sie

ve N

um

be

r (p

hi

Va

lue

)B

A-1

0-0

2 W

eig

ht

Pe

rcen

tsG

rave

l &

Sa

nd

Tota

l (%

)

87


1 (A) -1.50 -2.50 26.18 66.36 5.41 2.05 100.00 89.89 7.33 2.78

2 (B) -2.50 -6.70 0.40 17.88 44.20 37.52 100.00 17.95 44.38 37.68

3 (C) -6.70 -8.70 0.82 23.98 58.93 16.27 100.00 24.18 59.42 16.41

4 (D) -8.70 -10.00 1.10 63.80 29.16 5.94 100.00 64.51 29.49 6.00

5 (E) -10.00 -14.10 4.23 92.25 3.12 0.39 100.00 96.33 3.26 0.41

6 (F) -14.10 -15.50 6.07 26.58 38.07 29.28 100.00 28.29 40.53 31.18

7 (G) -15.50 -16.50 28.51 70.12 1.12 0.26 100.00 98.08 1.56 0.36

8 (H) -16.50 -17.50 36.64 60.44 2.11 0.82 100.00 95.39 3.32 1.29

9 (I) -17.50 -19.50 12.69 37.69 26.22 23.40 100.00 43.17 30.03 26.80

10 (J) -19.50 -21.20 20.57 74.90 3.83 0.70 100.00 94.30 4.82 0.88

11 (K) -21.20 -25.20 7.64 37.31 38.42 16.63 100.00 40.39 41.60 18.01

12 (L) -25.20 -26.00 0.02 58.00 39.80 2.17 100.00 58.01 39.81 2.17

13 (M) -26.00 -26.50 20.17 77.16 2.39 0.28 100.00 96.66 3.00 0.35

14 (N) -27.10 -30.00 5.54 42.47 36.46 15.53 100.00 44.96 38.60 16.45

15 (O) -30.00 -35.00 4.12 47.41 31.91 16.55 100.00 49.45 33.28 17.27

16 (P) -35.00 -40.00 6.29 48.86 37.66 7.19 100.00 52.14 40.19 7.67

17 (Q) -40.00 -43.60 28.97 61.70 8.07 1.26 100.00 86.86 11.36 1.77

18 (R) -43.60 -49.50 0.28 53.06 39.76 6.91 100.00 53.20 39.87 6.93

19 (S) -49.50 -53.00 0.39 95.69 3.70 0.21 100.00 96.07 3.72 0.22

20 (T) -53.00 -56.50 13.01 85.83 1.06 0.10 100.00 98.67 1.22 0.11

21 (U) -56.50 -59.10 0.17 32.82 63.45 3.56 100.00 32.88 63.56 3.56

22 (V) -59.10 -67.60 0.34 93.24 6.10 0.32 100.00 93.56 6.12 0.32

23 (W) -67.60 -69.00 0.03 1.55 71.10 27.32 100.00 1.55 71.12 27.33

24 (X) -69.50 -70.50 0.02 15.66 77.84 6.48 100.00 15.66 77.85 6.48

25 (Y) -70.50 -75.00 1.79 97.68 0.50 0.03 100.00 99.46 0.51 0.03

26 (Z) -69.00 -69.50 0.00 85.50 13.81 0.69 100.00 85.50 13.81 0.69

27 (AA) -75.00 -77.50 13.07 86.64 0.27 0.02 100.00 99.67 0.31 0.03

28 (BB) -77.50 -78.50 0.29 98.15 1.51 0.04 100.00 98.44 1.52 0.05

29 (CC) -78.50 -80.00 27.49 72.14 0.32 0.05 100.00 99.49 0.44 0.07

30 (DD) -80.00 -81.00 3.19 95.75 0.96 0.10 100.00 98.90 0.99 0.11

31 (EE) -81.00 -82.00 64.37 33.09 2.26 0.28 100.00 92.89 6.33 0.78

32 (FF) -82.00 -90.00 15.33 56.60 24.04 4.02 100.00 66.85 28.40 4.75

33 (GG) -90.00 -98.40 9.77 59.51 23.96 6.76 100.00 65.95 26.56 7.50

34 (HH) -98.40 -100.00 17.11 80.26 2.26 0.37 100.00 96.82 2.73 0.45

35 (II) -100.00 -102.70 29.80 60.05 8.66 1.49 100.00 85.54 12.33 2.13



88


36 (JJ) -102.70 -104.00 26.13 53.93 15.02 4.92 100.00 73.01 20.33 6.66

37 (KK) -104.00 -105.00 3.46 94.99 1.35 0.21 100.00 98.39 1.39 0.21

38 (LL) -105.00 -107.00 8.14 90.82 0.88 0.16 100.00 98.87 0.96 0.18

39 (MM) -107.00 -108.00 1.58 94.64 3.41 0.37 100.00 96.16 3.46 0.38

40 (NN) -108.00 -109.50 28.95 68.06 2.66 0.33 100.00 95.79 3.74 0.46

41 (OO) -109.50 -111.80 7.97 89.33 2.27 0.43 100.00 97.07 2.47 0.47

42 (PP) -111.80 -114.50 0.00 97.91 2.09 0.00 100.00 97.91 2.09 0.00

43 (QQ) -114.50 -119.00 0.00 88.05 8.79 3.17 100.00 88.05 8.79 3.17

44 (RR) -119.00 -121.00 0.00 57.70 30.09 12.21 100.00 57.70 30.09 12.21

45 (SS) -121.00 -131.70 0.00 73.46 24.77 1.77 100.00 73.46 24.77 1.77

46 (TT) -131.70 -132.60 0.00 23.14 64.65 12.21 100.00 23.14 64.65 12.21

47 (UU) -132.60 -136.00 0.00 62.25 35.83 1.92 100.00 62.25 35.83 1.92

48 (VV) -136.00 -140.00 0.00 61.79 36.13 2.08 100.00 61.79 36.13 2.08

49 (WW) -140.00 -146.40 0.00 55.74 40.99 3.27 100.00 55.74 40.99 3.27

50 (XX) -146.40 -149.20 0.00 39.71 54.35 5.94 100.00 39.71 54.35 5.94

51 (YY) -149.20 -159.00 0.00 51.84 44.32 3.84 100.00 51.84 44.32 3.84

52 (ZZ) -159.00 -160.00 0.00 10.09 76.76 13.15 100.00 10.09 76.76 13.15

53 (AAA) -160.00 -167.00 0.00 30.59 66.31 3.10 100.00 30.59 66.31 3.10

54 (BBB) -167.00 -177.30 0.00 45.32 50.53 4.15 100.00 45.32 50.53 4.15

55 (CCC) -177.30 -184.00 40.62 31.85 17.60 9.93 100.00 53.64 29.64 16.72

56 (DDD) -184.00 -190.00 38.77 38.62 19.43 3.17 100.00 63.08 31.74 5.18

57 (EEE) -190.00 -192.20 69.49 27.31 2.67 0.53 100.00 89.51 8.74 1.74

58 (FFF) -192.20 -200.00 2.04 21.82 46.06 30.08 100.00 22.28 47.02 30.71

59 (GGG) -200.00 -205.20 0.01 2.51 84.68 12.80 100.00 2.51 84.69 12.80

60 (HHH) -205.20 -208.00 1.82 33.95 40.83 23.40 100.00 34.58 41.59 23.83

61 (II I) -208.00 -211.00 0.68 23.00 50.74 25.59 100.00 23.15 51.08 25.76

62 (JJJ) -211.00 -215.00 17.72 55.54 22.18 4.56 100.00 67.50 26.96 5.54

63 (KKK) -220.00 -222.80 0.13 36.95 41.93 21.00 100.00 36.99 41.98 21.02

64 (LLL) -222.80 -225.00 7.07 57.94 31.00 3.99 100.00 62.34 33.36 4.29

65 (MMM) -225.00 -227.00 9.81 88.49 1.48 0.21 100.00 98.12 1.64 0.23

66 (NNN) -227.00 -230.00 0.03 97.59 2.19 0.19 100.00 97.62 2.19 0.19

67 (OOO) -230 -233.3 0.00 97.17 2.59 0.23 100.00 97.17 2.59 0.23

68 (PPP) -233.3 -237 31.33 37.34 21.96 9.37 100.00 54.37 31.99 13.64

69 (QQQ) -237 -240 13.70 4.81 45.04 36.45 100.00 5.58 52.19 42.24



89

Tota

l W

eig

ht

Sam

ple

ID

5 (φ

= -

2)10

(φ

= -

1)18

(φ

= 0

)35

(φ

= 1

)60

(φ

= 2

)12

0 (φ

= 3

)23

0 (φ

= 4

)Si

lt (

φ ≥

5)

Cla

y (φ

≥ 5

)(G

ram

s)

1 (A

)-0

.60

-4.0

029

.51

8.63

6.28

16.6

795

.90

102.

6536

.24

67.6

161

.98

425.

47

2 (B

)-4

.00

-9.0

018

.49

7.68

10.4

527

.67

121.

3712

6.35

40.2

953

.70

24.6

843

0.68

3 (C

)-9

.00

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500.

340.

965.

8646

.43

215.

5898

.18

13.4

07.

481.

1238

9.35

4 (D

)-1

0.50

-12.

3010

8.65

23.3

120

.76

38.5

810

6.23

92.2

430

.17

25.5

65.

1445

0.64

5 (E

)-1

2.30

-19.

0032

.27

16.4

618

.77

32.4

893

.14

96.3

645

.06

85.6

526

.65

446.

84

6 (F

)-1

9.00

-19.

5027

6.06

81.6

251

.98

30.3

234

.54

24.1

211

.10

5.92

0.84

516.

50

7 (G

)-1

9.50

-23.

6087

.69

17.7

619

.04

32.1

390

.98

92.4

642

.36

71.7

225

.82

479.

96

8 (H

)-2

3.60

-29.

0050

.10

16.5

217

.31

31.5

893

.32

94.2

842

.63

76.8

427

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450.

35

9 (I

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9.00

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5029

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13.9

615

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26.2

281

.55

92.2

146

.63

106.

3338

.56

450.

23

10 (

J)-3

2.50

-39.

0014

2.23

14.0

515

.26

25.2

277

.45

86.2

443

.55

101.

2239

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544.

30

11 (

K)-3

9.25

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0053

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12.4

012

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22.3

469

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77.9

339

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90.1

230

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408.

92

12 (

L)-4

9.00

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0065

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14.9

616

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29.0

988

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90.2

740

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93.4

937

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477.

27

13 (

M)

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00-5

9.00

33.7

714

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16.2

327

.20

82.2

487

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43.2

310

9.11

36.6

045

0.97

14 (

N)

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00-6

1.70

4.20

7.25

20.0

932

.44

72.7

314

6.61

72.3

038

.60

5.68

399.

90

15 (

O)

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70-6

4.00

0.00

0.04

0.15

5.01

171.

0616

1.66

36.9

621

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4.20

400.

09

16 (

P)-6

4.00

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700.

000.

120.

180.

424.

0411

9.67

135.

0615

3.90

24.4

343

7.82

17 (

Q)

-66.

70-6

8.00

1.47

2.81

2.87

7.94

23.1

233

.35

111.

3822

5.92

21.1

843

0.04

18 (

R)

-68.

00-7

4.00

30.5

615

.40

15.2

224

.64

73.5

185

.48

41.4

610

4.54

42.6

443

3.45

19 (

S)-7

4.00

-79.

0034

.60

14.0

515

.29

25.1

770

.64

77.4

637

.95

109.

0344

.34

428.

53

20 (

T)-7

9.00

-87.

8031

.90

17.6

318

.71

30.9

570

.86

66.7

237

.51

114.

0544

.14

432.

47

21 (

U)

-87.

80-8

9.00

0.68

1.15

1.19

2.69

12.2

034

.65

80.6

825

0.46

29.7

641

3.46

22 (

V)

-89.

00-9

3.20

201.

2743

.07

37.1

156

.64

118.

6063

.76

25.2

313

.76

1.66

561.

10

23 (

W)

-93.

20-9

7.40

302.

0361

.59

63.1

168

.26

87.1

024

.66

9.10

15.0

92.

4263

3.36

24 (

X)-9

7.40

-98.

500.

000.

000.

040.

078.

5722

0.45

78.9

823

.71

2.63

334.

45

25 (

Y)-9

8.50

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700.

000.

080.

050.

060.

992.

3643

.96

106.

3611

.25

165.

11

De

pth

(fe

et

fro

m s

urf

ace

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Pan

(p

hi

Va

lue

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eve

Nu

mb

er

(ph

i V

alu

e)

CA-1

1-01

Sam

ple

Mas

ses

90

Tota

l W

eig

ht

Sam

ple

ID

5 (φ

= -

2)10

(φ

= -

1)18

(φ

= 0

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(φ

= 1

)60

(φ

= 2

)12

0 (φ

= 3

)23

0 (φ

= 4

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lt (

φ ≥

5)

Cla

y (φ

≥ 5

)(G

ram

s)

26 (

Z)-9

9.70

-101

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45.3

218

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23.0

160

.23

117.

9172

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28.5

528

.44

5.28

400.

30

27 (

AA

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01.7

0-1

06.0

067

.88

10.8

113

.35

24.0

580

.57

83.1

138

.27

82.6

543

.81

444.

50

28 (

BB

)-1

06.0

0-1

10.7

035

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11.4

113

.54

26.6

793

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97.2

638

.52

89.2

554

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461.

36

29 (

CC)

-110

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-112

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42.6

840

.14

44.9

769

.47

140.

8638

.37

11.4

49.

223.

3540

0.50

30 (

DD

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12.7

0-1

15.0

07.

323.

844.

7426

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280.

354

11.5

10.1

21.

5940

0.09

31 (

EE)

-115

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-119

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25.4

410

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10.2

320

.57

86.7

810

6.97

43.9

83.5

944

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431.

67

32 (

FF)

-119

.00

-121

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93.6

831

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35.1

756

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116.

9350

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7.83

6.51

1.32

400.

38

33 (

GG

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21.5

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012

1.50

26.9

133

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76.2

710

8.47

23.0

14.

665.

340.

9540

0.69

34 (

HH

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55.5

556

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68.1

210

7.65

29.2

74.

093.

470.

6540

0.98

35 (

II)

-125

.50

-127

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0.20

1.24

2.34

37.4

828

6.49

64.6

86.

385.

881.

0840

5.77

36 (

JJ)

-127

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-129

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96.0

237

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52.3

99.9

886

.87

16.8

25.

35.

350.

9840

0.65

37 (

KK)

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0.11

0.5

3.64

86.4

417

0.57

45.6

25.

555.

971.

3731

9.77

38 (

LL)

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0.29

00.

011.

0734

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17.5

417

6.77

16.3

526

7.40

39 (

MM

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34.0

0-1

37.0

018

.74

20.5

23.8

351

.37

167.

1896

.26

14.5

16.

791.

0140

0.19

40 (

NN

)-1

37.0

0-1

39.0

010

9.33

32.7

928

.14

40.0

293

.69

60.6

620

.71

12.9

02.

0040

0.24

41 (

OO

)-1

39.0

0-1

46.8

032

.28

15.9

21.4

158

.39

165.

4955

.68

149.

821.

3937

4.36

42 (

PP)

-146

.80

-153

.00

12.0

44.

324.

4311

.62

57.0

883

49.6

134.

2362

.35

418.

67

43 (

QQ

)-1

53.0

0-1

59.0

01.

821.

943.

088.

8746

.06

69.9

537

.23

191.

7880

.47

441.

20

44 (

RR

)-1

59.0

0-1

64.3

00.

971.

632.

446.

7131

.755

.86

33.1

516

9.71

87.2

038

9.37

45 (

SS)

-164

.30

-166

.50

0.00

0.04

0.02

0.23

3.02

7.34

9.94

303.

5241

.82

365.

93

46 (

TT)

-166

.50

-169

.00

0.00

00

0.4

2.81

3.6

9.85

338.

5451

.71

406.

91

47 (

UU

)-1

69.0

0-1

72.9

030

.95

3.81

5.05

14.9

467

.43

92.9

798

.08

72.4

322

.26

407.

92

48 (

VV

)-1

72.9

0-1

74.5

010

6.00

27.9

925

.28

30.3

542

.86

45.8

573

.63

72.4

514

.33

438.

74

49 (

WW

)-1

74.5

0-1

75.5

026

.39

20.2

127

.71

39.1

247

.06

46.6

268

.61

93.2

819

.12

388.

12

50 (

XX)

-175

.50

-177

.60

104.

6231

.53

29.5

534

.37

44.9

445

.25

68.2

173

.51

13.6

644

5.64

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

CA-1

1-01

Sam

ple

Mas

ses

91

Sam

ple

ID

5 (φ

= -

2 )

10 (

φ =

-1)

18 (

φ =

0)

35 (

φ =

1)

60 (

φ =

2)

120

(φ =

3)

230

(φ =

4)

Silt

(φ

≥ 5

)Cl

ay

(φ ≥

5)

Sam

ple

To

tal

(%)

1 (A

)-0

.60

-4.0

06.

942.

031.

483.

9222

.54

24.1

38.

5269

.54

15.8

914

.57

100.

00

2 (B

)-4

.00

-9.0

04.

291.

782.

436.

4228

.18

29.3

49.

3581

.80

12.4

75.

7310

0.00

3 (C

)-9

.00

-10.

500.

090.

251.

5111

.93

55.3

725

.22

3.44

97.7

91.

920.

2910

0.00

4 (D

)-1

0.50

-12.

3024

.11

5.17

4.61

8.56

23.5

720

.47

6.69

93.1

95.

671.

1410

0.00

5 (E

)-1

2.30

-19.

007.

223.

684.

207.

2720

.84

21.5

610

.08

74.8

719

.17

5.96

100.

00

6 (F

)-1

9.00

-19.

5053

.45

15.8

010

.06

5.87

6.69

4.67

2.15

98.6

91.

150.

1610

0.00

7 (G

)-1

9.50

-23.

6018

.27

3.70

3.97

6.69

18.9

619

.26

8.83

79.6

814

.94

5.38

100.

00

8 (H

)-2

3.60

-29.

0011

.12

3.67

3.84

7.01

20.7

220

.93

9.47

76.7

717

.06

6.17

100.

00

9 (I

)-2

9.00

-32.

506.

583.

103.

375.

8218

.11

20.4

810

.36

67.8

223

.62

8.57

100.

00

10 (

J)-3

2.50

-39.

0026

.13

2.58

2.80

4.63

14.2

315

.84

8.00

74.2

218

.60

7.18

100.

00

11 (

K)-3

9.25

-49.

0013

.17

3.03

3.16

5.46

17.0

619

.06

9.55

70.5

022

.04

7.46

100.

00

12 (

L)-4

9.00

-54.

0013

.74

3.13

3.47

6.10

18.5

618

.91

8.56

72.4

719

.59

7.94

100.

00

13 (

M)

-54.

00-5

9.00

7.49

3.27

3.60

6.03

18.2

419

.48

9.59

67.6

924

.19

8.12

100.

00

14 (

N)

-59.

00-6

1.70

1.05

1.81

5.02

8.11

18.1

936

.66

18.0

888

.93

9.65

1.42

100.

00

15 (

O)

-61.

70-6

4.00

0.00

0.01

0.04

1.25

42.7

640

.41

9.24

93.7

05.

251.

0510

0.00

16 (

P)-6

4.00

-66.

700.

000.

030.

040.

100.

9227

.33

30.8

559

.27

35.1

55.

5810

0.00

17 (

Q)

-66.

70-6

8.00

0.34

0.65

0.67

1.85

5.38

7.76

25.9

042

.54

52.5

34.

9310

0.00

18 (

R)

-68.

00-7

4.00

7.05

3.55

3.51

5.68

16.9

619

.72

9.57

66.0

424

.12

9.84

100.

00

19 (

S)-7

4.00

-79.

008.

073.

283.

575.

8716

.48

18.0

88.

8664

.21

25.4

410

.35

100.

00

20 (

T)-7

9.00

-87.

807.

384.

084.

337.

1616

.38

15.4

38.

6763

.42

26.3

710

.21

100.

00

21 (

U)

-87.

80-8

9.00

0.16

0.28

0.29

0.65

2.95

8.38

19.5

132

.23

60.5

87.

2010

0.00

22 (

V)

-89.

00-9

3.20

35.8

77.

686.

6110

.09

21.1

411

.36

4.50

97.2

52.

450.

3010

0.00

23 (

W)

-93.

20-9

7.40

47.6

99.

729.

9610

.78

13.7

53.

891.

4497

.24

2.38

0.38

100.

00

24 (

X)-9

7.40

-98.

500.

000.

000.

010.

022.

5665

.91

23.6

192

.12

7.09

0.79

100.

00

25 (

Y)-9

8.50

-99.

700.

000.

050.

030.

040.

601.

4326

.62

28.7

764

.42

6.81

100.

00

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

Gra

vel

& S

an

d

Tota

l (%

)

CA-1

1-01

Sam

ple

Wei

ght

Perc

ent

92

Sam

ple

ID

5 (φ

= -

2 )

10 (

φ =

-1)

18 (

φ =

0)

35 (

φ =

1)

60 (

φ =

2)

120

(φ =

3)

230

(φ =

4)

Silt

(φ

≥ 5

)Cl

ay

(φ ≥

5)

Sam

ple

To

tal

(%)

26 (

Z)-9

9.70

-101

.70

11.3

24.

715.

7515

.05

29.4

618

.16

7.13

91.5

87.

101.

3210

0.00

27 (

AA

)-1

01.7

0-1

06.0

015

.27

2.43

3.00

5.41

18.1

318

.70

8.61

71.5

518

.59

9.86

100.

00

28 (

BB

)-1

06.0

0-1

10.7

07.

782.

472.

935.

7820

.37

21.0

88.

3568

.77

19.3

511

.89

100.

00

29 (

CC)

-110

.70

-112

.70

10.6

610

.02

11.2

317

.35

35.1

79.

582.

8696

.86

2.30

0.84

100.

00

30 (

DD

)-1

12.7

0-1

15.0

01.

830.

961.

186.

6770

.06

13.5

02.

8797

.07

2.53

0.40

100.

00

31 (

EE)

-115

.00

-119

.00

5.89

2.36

2.37

4.77

20.1

024

.78

10.1

770

.44

19.3

610

.20

100.

00

32 (

FF)

-119

.00

-121

.50

23.4

07.

858.

7814

.14

29.2

012

.71

1.96

98.0

41.

630.

3310

0.00

33 (

GG

)-1

21.5

0-1

24.0

030

.32

6.72

8.38

19.0

327

.07

5.74

1.16

98.4

31.

330.

2410

0.00

34 (

HH

)-1

24.0

0-1

25.5

018

.92

13.8

514

.04

16.9

926

.85

7.30

1.02

98.9

70.

870.

1610

0.00

35 (

II)

-125

.50

-127

.50

0.05

0.31

0.58

9.24

70.6

015

.94

1.57

98.2

81.

450.

2710

0.00

36 (

JJ)

-127

.50

-129

.00

23.9

79.

2413

.05

24.9

521

.68

4.20

1.32

98.4

21.

340.

2410

0.00

37 (

KK)

-129

.00

-129

.90

0.03

0.16

1.14

27.0

353

.34

14.2

71.

7497

.70

1.87

0.43

100.

00

38 (

LL)

-129

.90

-134

.00

0.11

0.00

0.00

0.40

13.0

57.

666.

5627

.78

66.1

16.

1210

0.00

39 (

MM

)-1

34.0

0-1

37.0

04.

685.

125.

9512

.84

41.7

824

.05

3.63

98.0

51.

700.

2510

0.00

40 (

NN

)-1

37.0

0-1

39.0

027

.32

8.19

7.03

10.0

023

.41

15.1

65.

1796

.28

3.22

0.50

100.

00

41 (

OO

)-1

39.0

0-1

46.8

08.

624.

255.

7215

.60

44.2

114

.87

3.74

97.0

12.

620.

3710

0.00

42 (

PP)

-146

.80

-153

.00

2.88

1.03

1.06

2.78

13.6

319

.82

11.8

553

.05

32.0

614

.89

100.

00

43 (

QQ

)-1

53.0

0-1

59.0

00.

410.

440.

702.

0110

.44

15.8

58.

4438

.29

43.4

718

.24

100.

00

44 (

RR

)-1

59.0

0-1

64.3

00.

250.

420.

631.

728.

1414

.35

8.51

34.0

243

.59

22.4

010

0.00

45 (

SS)

-164

.30

-166

.50

0.00

0.01

0.01

0.06

0.83

2.01

2.72

5.63

82.9

411

.43

100.

00

46 (

TT)

-166

.50

-169

.00

0.00

0.00

0.00

0.10

0.69

0.88

2.42

4.09

83.2

012

.71

100.

00

47 (

UU

)-1

69.0

0-1

72.9

07.

590.

931.

243.

6616

.53

22.7

924

.04

76.7

917

.75

5.46

100.

00

48 (

VV

)-1

72.9

0-1

74.5

024

.16

6.38

5.76

6.92

9.77

10.4

516

.78

80.2

216

.51

3.27

100.

00

49 (

WW

)-1

74.5

0-1

75.5

06.

805.

217.

1410

.08

12.1

312

.01

17.6

871

.04

24.0

34.

9310

0.00

50 (

XX)

-175

.50

-177

.60

23.4

87.

086.

637.

7110

.08

10.1

515

.31

80.4

416

.50

3.07

100.

00

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

Gra

vel

& S

an

d

Tota

l (%

)

CA-1

1-01

Sam

ple

Wei

ght

Perc

ent

93


1 (A) -0.60 -4.00 8.96 60.58 15.89 14.57 100.00 66.54 17.46 16.00

2 (B) -4.00 -9.00 6.08 75.72 12.47 5.73 100.00 80.62 13.28 6.10

3 (C) -9.00 -10.50 0.33 97.46 1.92 0.29 100.00 97.78 1.93 0.29

4 (D) -10.50 -12.30 29.28 63.90 5.67 1.14 100.00 90.37 8.02 1.61

5 (E) -12.30 -19.00 10.91 63.96 19.17 5.96 100.00 71.79 21.51 6.69

6 (F) -19.00 -19.50 69.25 29.44 1.15 0.16 100.00 95.74 3.73 0.53

7 (G) -19.50 -23.60 21.97 57.71 14.94 5.38 100.00 73.96 19.15 6.89

8 (H) -23.60 -29.00 14.79 61.98 17.06 6.17 100.00 72.74 20.02 7.24

9 (I) -29.00 -32.50 9.68 58.14 23.62 8.57 100.00 64.37 26.15 9.48

10 (J) -32.50 -39.00 28.71 45.51 18.60 7.18 100.00 63.84 26.09 10.07

11 (K) -39.25 -49.00 16.21 54.29 22.04 7.46 100.00 64.79 26.30 8.90

12 (L) -49.00 -54.00 16.88 55.59 19.59 7.94 100.00 66.88 23.57 9.55

13 (M) -54.00 -59.00 10.75 56.94 24.19 8.12 100.00 63.80 27.11 9.09

14 (N) -59.00 -61.70 2.86 86.06 9.65 1.42 100.00 88.60 9.94 1.46

15 (O) -61.70 -64.00 0.01 93.69 5.25 1.05 100.00 93.70 5.25 1.05

16 (P) -64.00 -66.70 0.03 59.24 35.15 5.58 100.00 59.26 35.16 5.58

17 (Q) -66.70 -68.00 1.00 41.54 52.53 4.93 100.00 41.96 53.06 4.97

18 (R) -68.00 -74.00 10.60 55.44 24.12 9.84 100.00 62.02 26.98 11.01

19 (S) -74.00 -79.00 11.35 52.86 25.44 10.35 100.00 59.63 28.70 11.67

20 (T) -79.00 -87.80 11.45 51.97 26.37 10.21 100.00 58.69 29.78 11.53

21 (U) -87.80 -89.00 0.44 31.78 60.58 7.20 100.00 31.92 60.84 7.23

22 (V) -89.00 -93.20 43.55 53.71 2.45 0.30 100.00 95.13 4.34 0.52

23 (W) -93.20 -97.40 57.41 39.82 2.38 0.38 100.00 93.51 5.59 0.90

24 (X) -97.40 -98.50 0.00 92.12 7.09 0.79 100.00 92.12 7.09 0.79

25 (Y) -98.50 -99.70 0.05 28.72 64.42 6.81 100.00 28.73 64.45 6.82

26 (Z) -99.70 -101.70 16.04 75.54 7.10 1.32 100.00 89.97 8.46 1.57

27 (AA) -101.70 -106.00 17.70 53.85 18.59 9.86 100.00 65.43 22.59 11.98

28 (BB) -106.00 -110.70 10.25 58.52 19.35 11.89 100.00 65.20 21.56 13.24

29 (CC) -110.70 -112.70 20.68 76.18 2.30 0.84 100.00 96.04 2.90 1.05

30 (DD) -112.70 -115.00 2.79 94.28 2.53 0.40 100.00 96.99 2.60 0.41

31 (EE) -115.00 -119.00 8.25 62.19 19.36 10.20 100.00 67.78 21.11 11.11

32 (FF) -119.00 -121.50 31.25 66.80 1.63 0.33 100.00 97.16 2.36 0.48

33 (GG) -121.50 -124.00 37.04 61.39 1.33 0.24 100.00 97.51 2.12 0.38

34 (HH) -124.00 -125.50 32.77 66.20 0.87 0.16 100.00 98.47 1.29 0.24

35 (II) -125.50 -127.50 0.35 97.93 1.45 0.27 100.00 98.28 1.45 0.27

36 (JJ) -127.50 -129.00 33.21 65.21 1.34 0.24 100.00 97.63 2.00 0.37

37 (KK) -129.00 -129.90 0.19 97.51 1.87 0.43 100.00 97.70 1.87 0.43

38 (LL) -129.90 -134.00 0.11 27.67 66.11 6.12 100.00 27.70 66.18 6.12

39 (MM) -134.00 -137.00 9.81 88.25 1.70 0.25 100.00 97.84 1.88 0.28

40 (NN) -137.00 -139.00 35.51 60.77 3.22 0.50 100.00 94.23 5.00 0.77

41 (OO) -139.00 -146.80 12.87 84.14 2.62 0.37 100.00 96.56 3.01 0.43

42 (PP) -146.80 -153.00 3.91 49.14 32.06 14.89 100.00 51.14 33.36 15.50

43 (QQ) -153.00 -159.00 0.85 37.44 43.47 18.24 100.00 37.76 43.84 18.39

44 (RR) -159.00 -164.30 0.67 33.35 43.59 22.40 100.00 33.58 43.88 22.55

45 (SS) -164.30 -166.50 0.01 5.62 82.94 11.43 100.00 5.62 82.95 11.43

46 (TT) -166.50 -169.00 0.00 4.09 83.20 12.71 100.00 4.09 83.20 12.71

47 (UU) -169.00 -172.90 8.52 68.27 17.75 5.46 100.00 74.62 19.41 5.97

48 (VV) -172.90 -174.50 30.54 49.68 16.51 3.27 100.00 71.52 23.77 4.70

49 (WW) -174.50 -175.50 12.01 59.03 24.03 4.93 100.00 67.09 27.31 5.60

50 (XX) -175.50 -177.60 30.55 49.89 16.50 3.07 100.00 71.83 23.75 4.41


Normalized SampleCA-11-01 Sample Particle Size Distribution

94

Tota

l W

eig

ht

Sam

ple

ID

5 (

φ =

-2

)1

0 (

φ =

-1

)1

8 (

φ =

0)

35

(φ

= 1

)6

0 (

φ =

2)

12

0 (

φ =

3)

23

0 (

φ =

4)

Silt

(φ

≥ 5

)C

lay

(φ ≥

5)

(Gra

ms)

8 -

18

A-8

.00

-18

.00

13

.47

10

.14

19

.16

63

.08

21

6.1

16

8.6

54

.48

4.7

70

.58

40

0.4

4

18

- 2

8 A

-18

.00

-28

.00

90

.13

26

.84

27

.60

59

.21

13

9.7

83

6.3

91

0.7

67

.71

2.1

64

00

.58

28

- 3

8 A

-1-2

8.0

0-3

3.0

01

28

.51

78

.44

74

.08

57

.41

38

.09

10

.92

4.3

47

.48

1.5

94

00

.86

28

- 3

8 A

-2-3

3.0

0-3

8.0

09

4.1

61

4.5

33

4.1

25

5.9

18

6.7

65

3.6

32

4.9

32

8.6

18

.25

40

0.9

0

38

- 4

8 A

-1-3

8.0

0-3

9.2

91

3.3

03

.96

7.7

32

1.9

98

4.9

55

6.3

11

7.6

28

4.2

51

02

.23

39

2.3

4

38

- 4

8 A

-2-3

9.2

9-4

1.6

90

.00

0.1

60

.12

1.1

23

.26

4.7

74

.20

31

5.9

36

4.1

93

93

.75

38

- 4

8 A

-3-4

1.6

9-4

2.9

80

.73

0.0

50

.24

0.6

73

.50

1.7

50

.61

13

1.7

42

32

.41

37

1.7

0

38

- 4

8 B

-42

.98

-48

.00

0.8

01

.03

2.7

97

.02

26

.95

43

.22

23

.17

16

1.9

11

46

.64

41

3.5

3

48

- 5

8 A

-48

.00

-52

.00

15

.55

16

.24

35

.67

45

.93

11

1.9

11

17

.84

33

.09

18

.82

5.8

54

00

.90

48

- 5

8 B

-52

.00

-56

.00

5.9

66

.33

7.2

81

1.0

14

3.0

19

1.4

35

4.8

21

32

.92

97

.75

45

0.5

1

48

- 5

8 C

-56

.00

-58

.00

2.4

95

.50

7.0

69

.89

40

.31

83

.33

50

.16

12

3.8

77

4.7

03

97

.31

58

- 6

8 A

-58

.00

-62

.34

18

.25

7.2

37

.24

10

.62

39

.97

81

.93

50

.47

15

3.1

67

4.2

64

43

.13

58

- 6

8 B

-62

.34

-65

.67

5.6

35

.68

7.6

21

0.7

94

1.3

18

5.4

15

3.4

21

67

.31

84

.62

46

1.7

9

58

- 6

8 C

-65

.67

-68

.00

5.1

65

.47

6.9

11

0.1

03

9.7

67

9.9

55

2.5

71

61

.11

74

.03

43

5.0

6

68

- 7

8 A

-68

.00

-72

.07

10

.58

5.8

76

.30

10

.40

40

.61

79

.33

52

.03

15

3.5

56

3.0

84

21

.75

68

- 7

8 B

-72

.07

-75

.02

6.5

56

.19

7.3

41

2.2

55

2.8

39

2.7

86

1.3

61

59

.92

70

.35

46

9.5

7

68

- 7

8 C

-75

.02

-78

.00

9.8

44

.90

6.1

41

2.7

75

2.8

59

8.7

75

7.7

01

61

.44

54

.16

45

8.5

7

78

- 8

8 A

-78

.00

-81

.54

41

.26

6.4

98

.33

14

.24

55

.53

10

9.4

36

5.3

41

48

.48

49

.75

49

8.8

5

78

- 8

8 B

-81

.54

-85

.08

5.4

47

.45

8.0

51

3.1

55

7.2

11

03

.74

62

.58

15

1.3

33

8.6

54

47

.60

78

- 8

8 C

-1-8

5.0

8-8

6.0

28

.82

4.9

66

.64

11

.42

50

.81

98

.32

58

.47

15

2.5

05

9.7

94

51

.73

78

- 8

8 C

-2-8

6.0

2-8

8.0

01

1.3

17

.03

7.2

21

0.9

64

6.4

98

9.7

25

3.3

71

29

.72

58

.75

41

4.5

7

88

- 9

8 A

-88

.00

-91

.37

17

.20

6.1

06

.72

10

.88

46

.86

92

.53

55

.25

15

6.1

15

8.9

04

50

.55

88

- 9

8 B

-91

.37

-95

.78

7.9

98

.53

9.8

51

6.4

05

4.0

57

7.8

75

4.6

31

48

.28

72

.76

45

0.3

6

88

- 9

8 C

-1-9

5.7

8-9

6.9

62

6.9

24

3.1

26

2.9

25

8.9

15

7.8

85

8.2

74

7.0

43

8.3

77

.65

40

1.0

8

88

- 9

8 C

-2-9

6.9

6-9

7.0

00

.10

0.6

82

.69

37

.57

16

4.0

58

1.1

96

7.2

07

8.2

41

8.4

84

50

.20

88

- 9

8 C

-3-9

7.0

0-9

8.0

03

.59

3.4

63

.15

3.5

91

8.7

71

67

.54

12

0.9

89

3.7

61

7.8

64

32

.70

98

- 1

08

A-9

8.0

0-1

03

.00

38

.39

17

.81

32

.69

10

6.3

01

28

.33

30

.42

19

.24

21

.81

5.9

64

00

.95

98

- 1

08

B-1

03

.00

-10

8.0

01

07

.69

49

.44

44

.84

76

.31

72

.12

21

.07

12

.98

13

.27

2.9

04

00

.62

10

8 -

11

8 A

-10

8.0

0-1

13

.54

3.1

61

2.0

43

7.2

59

4.5

22

06

.63

30

.33

7.3

08

.13

1.3

34

00

.69

10

8 -

11

8 B

-11

3.5

4-1

18

.00

6.5

61

.10

1.1

21

2.8

13

17

.36

43

.24

11

.37

5.8

31

.00

40

0.3

9

11

8 -

12

8 A

-11

8.0

0-1

23

.00

5.9

46

.56

14

.23

90

.20

24

0.3

93

0.3

16

.37

5.8

60

.99

40

0.8

5

11

8 -

12

8 B

-12

3.0

0-1

28

.00

32

.83

35

.05

60

.05

14

7.9

19

5.9

81

8.6

54

.52

4.6

90

.97

40

0.6

5

12

8 -

13

8 A

-12

8.0

0-1

33

.00

0.9

90

.37

5.1

44

8.4

91

58

.58

15

8.4

41

7.7

19

.63

1.3

04

00

.65

12

8 -

13

8 B

-1-1

33

.00

-13

4.3

10

.00

0.1

10

.56

2.5

71

11

.29

22

3.3

64

6.6

91

1.8

84

.26

40

0.7

2

12

8 -

13

8 B

-2-1

34.3

1-1

35

.50

0.0

00

.15

0.3

91

.65

10

7.1

71

69

.63

73

.66

86

.22

11

.98

45

0.8

5

12

8 -

13

8 B

-3-1

35.5

0-1

35

.58

0.0

00

.00

0.0

30

.40

8.5

73

3.0

97

5.7

32

73

.57

36

.65

42

8.0

4

De

pth

(fe

et

fro

m s

urf

ace

)

Pa

n (

ph

i V

alu

e)

Sie

ve N

um

be

r (p

hi

Va

lue

)K

A-1

2-0

2 S

amp

le M

asse

s

95

Tota

l W

eig

ht

Sam

ple

ID

5 (

φ =

-2

)1

0 (

φ =

-1

)1

8 (

φ =

0)

35

(φ

= 1

)6

0 (

φ =

2)

12

0 (

φ =

3)

23

0 (

φ =

4)

Silt

(φ

≥ 5

)C

lay

(φ ≥

5)

(Gra

ms)

12

8 -

13

8 B

-4-1

35

.58

-13

8.0

00

.18

0.7

61

.27

11

.67

23

3.0

91

15

.25

20

.83

15

.21

2.1

84

00

.44

13

8 -

14

8 A

-13

8.0

0-1

43

.00

0.0

70

.16

0.1

10

.56

82

.77

27

2.8

93

1.0

91

1.5

51

.52

40

0.7

2

13

8 -

14

8 B

-14

3.0

0-1

48

.00

0.0

00

.29

0.5

52

.66

10

6.6

12

24

.93

38

.80

23

.80

3.1

14

00

.75

14

8 -

15

8 A

-14

8.0

0-1

53

.00

0.0

00

.00

0.0

00

.00

7.2

12

1.2

09

1.9

02

61

.58

18

.87

40

0.7

6

14

8 -

15

8 B

-15

3.0

0-1

58

.00

0.0

00

.09

0.0

00

.04

5.2

64

8.8

11

83

.25

15

0.3

71

2.7

04

00

.52

15

8 -

16

8 A

-15

8.0

0-1

61

.50

0.0

00

.00

0.0

80

.96

3.5

83

.74

4.6

63

47

.92

90

.22

45

1.1

6

15

8 -

16

8 B

-16

1.5

0-1

65

.00

0.0

00

.00

0.0

00

.10

7.2

47

.69

6.1

72

14

.34

12

5.6

23

61

.16

15

8 -

16

8 C

-16

5.0

0-1

68

.00

0.0

00

.00

0.0

30

.17

1.5

13

.01

5.0

62

35

.56

15

3.4

73

98

.81

16

8 -

17

8 A

-16

8.0

0-1

73

.00

0.0

00

.00

0.0

10

.43

2.8

54

.12

3.9

33

11

.53

82

.06

40

4.9

3

16

8 -

17

8 B

-1-1

73

.00

-17

5.5

60

.00

0.0

00

.09

0.8

73

.05

2.2

41

03

.94

29

3.5

63

3.1

74

36

.92

16

8 -

17

8 B

-2-1

75

.56

-17

8.0

00

.00

0.0

00

.18

0.6

11

.25

0.9

19

.64

33

9.9

43

3.5

03

86

.03

17

8 -

18

8 A

-1-1

78

.00

-18

1.7

00

.00

0.0

00

.09

0.2

20

.72

29

.54

15

8.1

42

25

.57

26

.38

44

0.6

6

17

8 -

18

8 A

-2-1

81

.70

-18

3.0

00

.00

0.0

61

.40

5.0

71

0.7

48

.78

8.3

21

49

.76

21

6.9

14

01

.04

17

8 -

18

8 B

-1-1

83

.00

-18

4.2

50

.00

0.0

00

.03

0.1

12

.43

12

.20

36

.87

22

0.8

31

03

.34

37

5.8

1

17

8 -

18

8 B

-2-1

84

.25

-18

5.1

90

.00

0.0

00

.10

0.1

30

.45

23

.30

65

.98

32

8.4

23

5.6

84

54

.06

17

8 -

18

8 B

-3-1

85

.19

-18

8.0

00

.00

0.0

00

.00

0.4

23

.76

5.8

35

.72

27

4.7

11

01

.10

39

1.5

4

18

8 -

19

8 A

-1-1

88

.00

-18

9.6

60

.00

0.0

00

.98

4.5

09

.54

9.8

71

2.5

71

97

.66

13

2.7

93

67

.91

18

8 -

19

8 A

-2-1

89

.66

-19

1.3

20

.00

0.0

00

.78

3.0

17

.59

7.7

19

.48

18

8.4

31

35

.93

35

2.9

3

18

8 -

19

8 B

-19

1.3

2-1

95

.23

0.0

00

.07

1.2

44

.02

10

.89

12

.62

14

.74

22

0.2

81

36

.29

40

0.1

5

18

8 -

19

8 C

-19

5.2

3-1

98

.00

0.0

00

.00

0.2

71

.44

5.6

96

.57

6.1

92

46

.04

17

1.6

74

37

.87

19

8 -

20

8 A

-19

8.0

0-2

03

.00

0.0

00

.60

4.0

01

0.0

32

1.4

52

1.7

61

7.5

01

16

.38

18

1.4

53

73

.17

19

8 -

20

8 B

-1-2

03

.00

-20

5.2

04

.21

3.5

38

.18

75

.58

23

5.4

14

7.5

11

0.8

81

1.3

33

.93

40

0.5

6

19

8 -

20

8 B

-2-2

05

.20

-20

8.0

00

.00

0.2

00

.55

4.8

11

6.7

31

2.5

41

0.7

93

10

.70

93

.71

45

0.0

3

20

8 -

21

8 A

-1-2

08

.00

-21

0.5

10

.34

1.1

42

.26

16

.61

65

.04

15

.65

7.0

32

35

.99

10

6.3

74

50

.43

20

8 -

21

8 A

-2-2

10

.51

-21

1.7

63

.98

5.8

91

6.8

74

6.0

22

44

.66

49

.94

17

.85

11

.91

3.3

64

00

.48

20

8 -

21

8 A

-3-2

11

.76

-21

3.0

00

.14

1.0

32

.67

11

.18

37

.77

19

.44

17

.36

18

4.5

69

5.4

43

69

.59

20

8 -

21

8 B

-21

3.0

0-2

18

.00

41

.28

20

.57

35

.04

11

4.2

11

41

.93

22

.24

21

.53

2.6

00

.87

40

0.2

6

21

8 -

22

8 A

-21

8.0

0-2

23

.00

8.2

17

.83

24

.59

12

0.2

51

86

.90

37

.38

5.8

48

.15

1.2

84

00

.43

21

8 -

22

8 B

-22

3.0

0-2

28

.00

41

.82

37

.18

56

.85

10

1.7

81

21

.58

24

.06

8.2

57

.87

1.0

94

00

.48

22

8 -

23

8 A

-22

8.0

0-2

33

.00

32

.95

5.6

41

5.4

88

0.0

81

71

.68

62

.03

13

.62

16

.30

3.0

04

00

.78

22

8 -

23

8 B

-23

3.0

0-2

38

.00

0.3

87

.35

13

.07

30

.26

22

1.6

26

9.9

42

0.9

93

1.0

75

.89

40

0.5

7

23

8 -

24

8 A

-23

8.0

0-2

43

.00

7.6

20

.04

0.3

02

.54

22

5.6

41

43

.61

11

.78

7.6

11

.19

40

0.3

3

23

8 -

24

8 B

-23

4.0

0-2

48

.00

50

.16

36

.81

51

.23

10

0.3

01

04

.58

26

.08

13

.58

14

.97

2.9

04

00

.61

24

8 -

25

9 A

-24

8.0

0-2

54

.00

19

7.4

73

6.4

52

8.1

64

2.6

05

0.6

11

5.8

81

3.4

81

3.1

32

.74

40

0.5

2

24

8 -

25

9 B

-25

4.0

0-2

59

.00

15

8.5

93

6.7

52

9.5

55

8.5

35

5.6

92

1.2

51

8.8

71

7.1

53

.79

40

0.1

7

De

pth

(fe

et

fro

m s

urf

ace

)

Pa

n (

ph

i V

alu

e)

Sie

ve N

um

be

r (p

hi

Va

lue

)K

A-1

2-0

2 S

amp

le M

asse

s

96

Sam

ple

ID

5 (

φ =

-2

)1

0 (

φ =

-1

)1

8 (

φ =

0)

35

(φ

= 1

)6

0 (

φ =

2)

12

0 (

φ =

3)

23

0 (

φ =

4)

Silt

(φ

≥ 5

)C

lay

(φ ≥

5)

Sam

ple

To

tal

(%)

8 -

18

A-8

.00

-18

.00

3.3

62

.53

4.7

81

5.7

55

3.9

71

7.1

41

.12

98

.66

1.1

90

.15

10

0.0

0

18

- 2

8 A

-18

.00

-28

.00

22

.50

6.7

06

.89

14

.78

34

.89

9.0

82

.69

97

.54

1.9

30

.54

10

0.0

0

28

- 3

8 A

-1-2

8.0

0-3

3.0

03

2.0

61

9.5

71

8.4

81

4.3

29

.50

2.7

21

.08

97

.74

1.8

70

.40

10

0.0

0

28

- 3

8 A

-2-3

3.0

0-3

8.0

02

3.4

93

.62

8.5

11

3.9

52

1.6

41

3.3

86

.22

90

.81

7.1

42

.06

10

0.0

0

38

- 4

8 A

-1-3

8.0

0-3

9.2

93

.39

1.0

11

.97

5.6

02

1.6

51

4.3

54

.49

52

.47

21

.47

26

.06

10

0.0

0

38

- 4

8 A

-2-3

9.2

9-4

1.6

90

.00

0.0

40

.03

0.2

80

.83

1.2

11

.07

3.4

68

0.2

31

6.3

01

00

.00

38

- 4

8 A

-3-4

1.6

9-4

2.9

80

.20

0.0

10

.06

0.1

80

.94

0.4

70

.16

2.0

33

5.4

46

2.5

31

00

.00

38

- 4

8 B

-42

.98

-48

.00

0.1

90

.25

0.6

71

.70

6.5

21

0.4

55

.60

25

.39

39

.15

35

.46

10

0.0

0

48

- 5

8 A

-48

.00

-52

.00

3.8

84

.05

8.9

01

1.4

62

7.9

12

9.3

98

.25

93

.85

4.6

91

.46

10

0.0

0

48

- 5

8 B

-52

.00

-56

.00

1.3

21

.41

1.6

22

.44

9.5

52

0.2

91

2.1

74

8.8

02

9.5

12

1.7

01

00

.00

48

- 5

8 C

-56

.00

-58

.00

0.6

31

.38

1.7

82

.49

10

.15

20

.97

12

.62

50

.02

31

.18

18

.80

10

0.0

0

58

- 6

8 A

-58

.00

-62

.34

4.1

21

.63

1.6

32

.40

9.0

21

8.4

91

1.3

94

8.6

83

4.5

61

6.7

61

00

.00

58

- 6

8 B

-62

.34

-65

.67

1.2

21

.23

1.6

52

.34

8.9

51

8.5

01

1.5

74

5.4

43

6.2

31

8.3

21

00

.00

58

- 6

8 C

-65

.67

-68

.00

1.1

91

.26

1.5

92

.32

9.1

41

8.3

81

2.0

84

5.9

53

7.0

31

7.0

21

00

.00

68

- 7

8 A

-68

.00

-72

.07

2.5

11

.39

1.4

92

.47

9.6

31

8.8

11

2.3

44

8.6

43

6.4

11

4.9

61

00

.00

68

- 7

8 B

-72

.07

-75

.02

1.3

91

.32

1.5

62

.61

11

.25

19

.76

13

.07

50

.96

34

.06

14

.98

10

0.0

0

68

- 7

8 C

-75

.02

-78

.00

2.1

51

.07

1.3

42

.78

11

.52

21

.54

12

.58

52

.98

35

.21

11

.81

10

0.0

0

78

- 8

8 A

-78

.00

-81

.54

8.2

71

.30

1.6

72

.85

11

.13

21

.94

13

.10

60

.26

29

.77

9.9

71

00

.00

78

- 8

8 B

-81

.54

-85

.08

1.2

21

.66

1.8

02

.94

12

.78

23

.18

13

.98

57

.56

33

.81

8.6

31

00

.00

78

- 8

8 C

-1-8

5.0

8-8

6.0

21

.95

1.1

01

.47

2.5

31

1.2

52

1.7

71

2.9

45

3.0

13

3.7

61

3.2

41

00

.00

78

- 8

8 C

-2-8

6.0

2-8

8.0

02

.73

1.7

01

.74

2.6

41

1.2

12

1.6

41

2.8

75

4.5

43

1.2

91

4.1

71

00

.00

88

- 9

8 A

-88

.00

-91

.37

3.8

21

.35

1.4

92

.41

10

.40

20

.54

12

.26

52

.28

34

.65

13

.07

10

0.0

0

88

- 9

8 B

-91

.37

-95

.78

1.7

71

.89

2.1

93

.64

12

.00

17

.29

12

.13

50

.92

32

.92

16

.16

10

0.0

0

88

- 9

8 C

-1-9

5.7

8-9

6.9

66

.71

10

.75

15

.69

14

.69

14

.43

14

.53

11

.73

88

.53

9.5

71

.91

10

0.0

0

88

- 9

8 C

-2-9

6.9

6-9

7.0

00

.02

0.1

50

.60

8.3

53

6.4

41

8.0

31

4.9

37

8.5

21

7.3

84

.11

10

0.0

0

88

- 9

8 C

-3-9

7.0

0-9

8.0

00

.83

0.8

00

.73

0.8

34

.34

38

.72

27

.96

74

.20

21

.67

4.1

31

00

.00

98

- 1

08

A-9

8.0

0-1

03

.00

9.5

74

.44

8.1

52

6.5

13

2.0

17

.59

4.8

09

3.0

75

.44

1.4

91

00

.00

98

- 1

08

B-1

03

.00

-10

8.0

02

6.8

81

2.3

41

1.1

91

9.0

51

8.0

05

.26

3.2

49

5.9

63

.31

0.7

21

00

.00

10

8 -

11

8 A

-10

8.0

0-1

13

.54

0.7

93

.00

9.3

02

3.5

95

1.5

77

.57

1.8

29

7.6

42

.03

0.3

31

00

.00

10

8 -

11

8 B

-11

3.5

4-1

18

.00

1.6

40

.27

0.2

83

.20

79

.26

10

.80

2.8

49

8.2

91

.46

0.2

51

00

.00

11

8 -

12

8 A

-11

8.0

0-1

23

.00

1.4

81

.64

3.5

52

2.5

05

9.9

77

.56

1.5

99

8.2

91

.46

0.2

51

00

.00

11

8 -

12

8 B

-12

3.0

0-1

28

.00

8.1

98

.75

14

.99

36

.92

23

.96

4.6

51

.13

98

.59

1.1

70

.24

10

0.0

0

12

8 -

13

8 A

-12

8.0

0-1

33

.00

0.2

50

.09

1.2

81

2.1

03

9.5

83

9.5

54

.42

97

.27

2.4

00

.32

10

0.0

0

12

8 -

13

8 B

-1-1

33

.00

-13

4.3

10

.00

0.0

30

.14

0.6

42

7.7

75

5.7

41

1.6

59

5.9

72

.96

1.0

61

00

.00

12

8 -

13

8 B

-2-1

34

.31

-13

5.5

00

.00

0.0

30

.09

0.3

72

3.7

73

7.6

21

6.3

47

8.2

21

9.1

22

.66

10

0.0

0

12

8 -

13

8 B

-3-1

35

.50

-13

5.5

80

.00

0.0

00

.01

0.0

92

.00

7.7

31

7.6

92

7.5

36

3.9

18

.56

10

0.0

0

De

pth

(fe

et

fro

m s

urf

ace

)

Pa

n (

ph

i V

alu

e)

Sie

ve N

um

be

r (p

hi

Va

lue

)K

A-1

2-0

2 S

amp

le W

eig

ht

Pe

rcen

tsG

rave

l &

Sa

nd

Tota

l (%

)

97

Sam

ple

ID

5 (

φ =

-2

)1

0 (

φ =

-1

)1

8 (

φ =

0)

35

(φ

= 1

)6

0 (

φ =

2)

12

0 (

φ =

3)

23

0 (

φ =

4)

Silt

(φ

≥ 5

)C

lay

(φ ≥

5)

Sam

ple

To

tal

(%)

12

8 -

13

8 B

-4-1

35

.58

-13

8.0

00

.04

0.1

90

.32

2.9

15

8.2

12

8.7

85

.20

95

.66

3.8

00

.54

10

0.0

0

13

8 -

14

8 A

-13

8.0

0-1

43

.00

0.0

20

.04

0.0

30

.14

20

.66

68

.10

7.7

69

6.7

42

.88

0.3

81

00

.00

13

8 -

14

8 B

-14

3.0

0-1

48

.00

0.0

00

.07

0.1

40

.66

26

.60

56

.13

9.6

89

3.2

95

.94

0.7

81

00

.00

14

8 -

15

8 A

-14

8.0

0-1

53

.00

0.0

00

.00

0.0

00

.00

1.8

05

.29

22

.93

30

.02

65

.27

4.7

11

00

.00

14

8 -

15

8 B

-15

3.0

0-1

58

.00

0.0

00

.02

0.0

00

.01

1.3

11

2.1

94

5.7

55

9.2

93

7.5

43

.17

10

0.0

0

15

8 -

16

8 A

-15

8.0

0-1

61

.50

0.0

00

.00

0.0

20

.21

0.7

90

.83

1.0

32

.89

77

.12

20

.00

10

0.0

0

15

8 -

16

8 B

-16

1.5

0-1

65

.00

0.0

00

.00

0.0

00

.03

2.0

02

.13

1.7

15

.87

59

.35

34

.78

10

0.0

0

15

8 -

16

8 C

-16

5.0

0-1

68

.00

0.0

00

.00

0.0

10

.04

0.3

80

.75

1.2

72

.45

59

.07

38

.48

10

0.0

0

16

8 -

17

8 A

-16

8.0

0-1

73

.00

0.0

00

.00

0.0

00

.11

0.7

01

.02

0.9

72

.80

76

.93

20

.27

10

0.0

0

16

8 -

17

8 B

-1-1

73

.00

-17

5.5

60

.00

0.0

00

.02

0.2

00

.70

0.5

12

3.7

92

5.2

26

7.1

97

.59

10

0.0

0

16

8 -

17

8 B

-2-1

75

.56

-17

8.0

00

.00

0.0

00

.05

0.1

60

.32

0.2

42

.50

3.2

68

8.0

68

.68

10

0.0

0

17

8 -

18

8 A

-1-1

78

.00

-18

1.7

00

.00

0.0

00

.02

0.0

50

.16

6.7

03

5.8

94

2.8

25

1.1

95

.99

10

0.0

0

17

8 -

18

8 A

-2-1

81

.70

-18

3.0

00

.00

0.0

10

.35

1.2

62

.68

2.1

92

.07

8.5

73

7.3

45

4.0

91

00

.00

17

8 -

18

8 B

-1-1

83

.00

-18

4.2

50

.00

0.0

00

.01

0.0

30

.65

3.2

59

.81

13

.74

58

.76

27

.50

10

0.0

0

17

8 -

18

8 B

-2-1

84

.25

-18

5.1

90

.00

0.0

00

.02

0.0

30

.10

5.1

31

4.5

31

9.8

17

2.3

37

.86

10

0.0

0

17

8 -

18

8 B

-3-1

85

.19

-18

8.0

00

.00

0.0

00

.00

0.1

10

.96

1.4

91

.46

4.0

27

0.1

62

5.8

21

00

.00

18

8 -

19

8 A

-1-1

88

.00

-18

9.6

60

.00

0.0

00

.27

1.2

22

.59

2.6

83

.42

10

.18

53

.72

36

.09

10

0.0

0

18

8 -

19

8 A

-2-1

89

.66

-19

1.3

20

.00

0.0

00

.22

0.8

52

.15

2.1

82

.69

8.1

05

3.3

93

8.5

21

00

.00

18

8 -

19

8 B

-19

1.3

2-1

95

.23

0.0

00

.02

0.3

11

.00

2.7

23

.15

3.6

81

0.8

95

5.0

53

4.0

61

00

.00

18

8 -

19

8 C

-19

5.2

3-1

98

.00

0.0

00

.00

0.0

60

.33

1.3

01

.50

1.4

14

.60

56

.19

39

.21

10

0.0

0

19

8 -

20

8 A

-19

8.0

0-2

03

.00

0.0

00

.16

1.0

72

.69

5.7

55

.83

4.6

92

0.1

93

1.1

94

8.6

21

00

.00

19

8 -

20

8 B

-1-2

03

.00

-20

5.2

01

.05

0.8

82

.04

18

.87

58

.77

11

.86

2.7

29

6.1

92

.83

0.9

81

00

.00

19

8 -

20

8 B

-2-2

05

.20

-20

8.0

00

.00

0.0

40

.12

1.0

73

.72

2.7

92

.40

10

.14

69

.04

20

.82

10

0.0

0

20

8 -

21

8 A

-1-2

08

.00

-21

0.5

10

.08

0.2

50

.50

3.6

91

4.4

43

.47

1.5

62

3.9

95

2.3

92

3.6

21

00

.00

20

8 -

21

8 A

-2-2

10

.51

-21

1.7

60

.99

1.4

74

.21

11

.49

61

.09

12

.47

4.4

69

6.1

92

.97

0.8

41

00

.00

20

8 -

21

8 A

-3-2

11

.76

-21

3.0

00

.04

0.2

80

.72

3.0

21

0.2

25

.26

4.7

02

4.2

44

9.9

42

5.8

21

00

.00

20

8 -

21

8 B

-21

3.0

0-2

18

.00

10

.31

5.1

48

.75

28

.53

35

.46

5.5

65

.38

99

.14

0.6

50

.22

10

0.0

0

21

8 -

22

8 A

-21

8.0

0-2

23

.00

2.0

51

.96

6.1

43

0.0

34

6.6

79

.33

1.4

69

7.6

52

.03

0.3

21

00

.00

21

8 -

22

8 B

-22

3.0

0-2

28

.00

10

.44

9.2

81

4.2

02

5.4

13

0.3

66

.01

2.0

69

7.7

61

.97

0.2

71

00

.00

22

8 -

23

8 A

-22

8.0

0-2

33

.00

8.2

21

.41

3.8

61

9.9

84

2.8

41

5.4

83

.40

95

.18

4.0

70

.75

10

0.0

0

22

8 -

23

8 B

-23

3.0

0-2

38

.00

0.0

91

.83

3.2

67

.55

55

.33

17

.46

5.2

49

0.7

77

.76

1.4

71

00

.00

23

8 -

24

8 A

-23

8.0

0-2

43

.00

1.9

00

.01

0.0

70

.63

56

.36

35

.87

2.9

49

7.8

01

.90

0.3

01

00

.00

23

8 -

24

8 B

-23

4.0

0-2

48

.00

12

.52

9.1

91

2.7

92

5.0

42

6.1

16

.51

3.3

99

5.5

43

.74

0.7

21

00

.00

24

8 -

25

9 A

-24

8.0

0-2

54

.00

49

.30

9.1

07

.03

10

.64

12

.64

3.9

63

.37

96

.04

3.2

80

.68

10

0.0

0

24

8 -

25

9 B

-25

4.0

0-2

59

.00

39

.63

9.1

87

.38

14

.63

13

.92

5.3

14

.72

94

.77

4.2

90

.95

10

0.0

0

De

pth

(fe

et

fro

m s

urf

ace

)

Pa

n (

ph

i V

alu

e)

Sie

ve N

um

be

r (p

hi

Va

lue

)K

A-1

2-0

2 S

amp

le W

eig

ht

Pe

rcen

tsG

rave

l &

Sa

nd

Tota

l (%

)

98


8 - 18 A -8.00 -18.00 5.90 92.77 1.19 0.15 100.00 98.58 1.27 0.15

18 - 28 A -18.00 -28.00 29.20 68.34 1.93 0.54 100.00 96.52 2.72 0.76

28 - 38 A-1 -28.00 -33.00 51.63 46.11 1.87 0.40 100.00 95.32 3.86 0.82

28 - 38 A-2 -33.00 -38.00 27.11 63.69 7.14 2.06 100.00 87.39 9.79 2.82

38 - 48 A-1 -38.00 -39.29 4.40 48.07 21.47 26.06 100.00 50.28 22.46 27.26

38 - 48 A-2 -39.29 -41.69 0.04 3.42 80.23 16.30 100.00 3.42 80.27 16.31

38 - 48 A-3 -41.69 -42.98 0.21 1.82 35.44 62.53 100.00 1.83 35.52 62.66

38 - 48 B -42.98 -48.00 0.44 24.94 39.15 35.46 100.00 25.05 39.33 35.62

48 - 58 A -48.00 -52.00 7.93 85.92 4.69 1.46 100.00 93.32 5.10 1.59

48 - 58 B -52.00 -56.00 2.73 46.07 29.51 21.70 100.00 47.36 30.33 22.31

48 - 58 C -56.00 -58.00 2.01 48.01 31.18 18.80 100.00 49.00 31.82 19.19

58 - 68 A -58.00 -62.34 5.75 42.93 34.56 16.76 100.00 45.55 36.67 17.78

58 - 68 B -62.34 -65.67 2.45 43.00 36.23 18.32 100.00 44.08 37.14 18.78

58 - 68 C -65.67 -68.00 2.44 43.51 37.03 17.02 100.00 44.60 37.96 17.44

68 - 78 A -68.00 -72.07 3.90 44.74 36.41 14.96 100.00 46.55 37.89 15.56

68 - 78 B -72.07 -75.02 2.71 48.25 34.06 14.98 100.00 49.59 35.01 15.40

68 - 78 C -75.02 -78.00 3.21 49.77 35.21 11.81 100.00 51.42 36.38 12.20

78 - 88 A -78.00 -81.54 9.57 50.69 29.77 9.97 100.00 56.06 32.92 11.03

78 - 88 B -81.54 -85.08 2.88 54.68 33.81 8.63 100.00 56.30 34.81 8.89

78 - 88 C-1 -85.08 -86.02 3.05 49.95 33.76 13.24 100.00 51.53 34.82 13.65

78 - 88 C-2 -86.02 -88.00 4.42 50.11 31.29 14.17 100.00 52.43 32.74 14.83

88 - 98 A -88.00 -91.37 5.17 47.11 34.65 13.07 100.00 49.68 36.54 13.79

88 - 98 B -91.37 -95.78 3.67 47.25 32.92 16.16 100.00 49.05 34.18 16.77

88 - 98 C-1 -95.78 -96.96 17.46 71.06 9.57 1.91 100.00 86.10 11.59 2.31

88 - 98 C-2 -96.96 -97.00 0.17 78.34 17.38 4.11 100.00 78.48 17.41 4.11

88 - 98 C-3 -97.00 -98.00 1.63 72.57 21.67 4.13 100.00 73.78 22.03 4.20

98 - 108 A -98.00 -103.00 14.02 79.06 5.44 1.49 100.00 91.94 6.33 1.73

98 - 108 B -103.00 -108.00 39.22 56.74 3.31 0.72 100.00 93.36 5.45 1.19

108 - 118 A -108.00 -113.54 3.79 93.85 2.03 0.33 100.00 97.55 2.11 0.35

108 - 118 B -113.54 -118.00 1.91 96.38 1.46 0.25 100.00 98.26 1.49 0.25

118 - 128 A -118.00 -123.00 3.12 95.17 1.46 0.25 100.00 98.24 1.51 0.25

118 - 128 B -123.00 -128.00 16.94 81.64 1.17 0.24 100.00 98.30 1.41 0.29

128 - 138 A -128.00 -133.00 0.34 96.93 2.40 0.32 100.00 97.26 2.41 0.33

128 - 138 B-1 -133.00 -134.31 0.03 95.94 2.96 1.06 100.00 95.97 2.97 1.06

128 - 138 B-2 -134.31 -135.50 0.03 78.19 19.12 2.66 100.00 78.21 19.13 2.66

128 - 138 B-3 -135.50 -135.58 0.00 27.53 63.91 8.56 100.00 27.53 63.91 8.56


Normalized SampleKA-12-02 Sample Particle Size Distribution

99


128 - 138 B-4 -135.58 -138.00 0.23 95.42 3.80 0.54 100.00 95.65 3.81 0.54

138 - 148 A -138.00 -143.00 0.06 96.68 2.88 0.38 100.00 96.74 2.88 0.38

138 - 148 B -143.00 -148.00 0.07 93.21 5.94 0.78 100.00 93.28 5.94 0.78

148 - 158 A -148.00 -153.00 0.00 30.02 65.27 4.71 100.00 30.02 65.27 4.71

148 - 158 B -153.00 -158.00 0.02 59.26 37.54 3.17 100.00 59.28 37.55 3.17

158 - 168 A -158.00 -161.50 0.00 2.89 77.12 20.00 100.00 2.89 77.12 20.00

158 - 168 B -161.50 -165.00 0.00 5.87 59.35 34.78 100.00 5.87 59.35 34.78

158 - 168 C -165.00 -168.00 0.00 2.45 59.07 38.48 100.00 2.45 59.07 38.48

168 - 178 A -168.00 -173.00 0.00 2.80 76.93 20.27 100.00 2.80 76.93 20.27

168 - 178 B-1 -173.00 -175.56 0.00 25.22 67.19 7.59 100.00 25.22 67.19 7.59

168 - 178 B-2 -175.56 -178.00 0.00 3.26 88.06 8.68 100.00 3.26 88.06 8.68

178 - 188 A-1 -178.00 -181.70 0.00 42.82 51.19 5.99 100.00 42.82 51.19 5.99

178 - 188 A-2 -181.70 -183.00 0.01 8.56 37.34 54.09 100.00 8.56 37.35 54.09

178 - 188 B-1 -183.00 -184.25 0.00 13.74 58.76 27.50 100.00 13.74 58.76 27.50

178 - 188 B-2 -184.25 -185.19 0.00 19.81 72.33 7.86 100.00 19.81 72.33 7.86

178 - 188 B-3 -185.19 -188.00 0.00 4.02 70.16 25.82 100.00 4.02 70.16 25.82

188 - 198 A-1 -188.00 -189.66 0.00 10.18 53.72 36.09 100.00 10.18 53.72 36.09

188 - 198 A-2 -189.66 -191.32 0.00 8.10 53.39 38.52 100.00 8.10 53.39 38.52

188 - 198 B -191.32 -195.23 0.02 10.87 55.05 34.06 100.00 10.88 55.06 34.06

188 - 198 C -195.23 -198 0.00 4.60 56.19 39.21 100.00 4.60 56.19 39.21

198 - 208 A -198 -203 0.16 20.03 31.19 48.62 100.00 20.06 31.24 48.70

198 - 208 B-1 -203 -205.2 1.93 94.26 2.83 0.98 100.00 96.12 2.88 1.00

198 - 208 B-2 -205.2 -208 0.04 10.09 69.04 20.82 100.00 10.10 69.07 20.83

208 - 218 A-1 -208 -210.51 0.33 23.66 52.39 23.62 100.00 23.74 52.56 23.69

208 - 218 A-2 -210.51 -211.76 2.46 93.72 2.97 0.84 100.00 96.09 3.05 0.86

208 - 218 A-3 -211.76 -213 0.32 23.92 49.94 25.82 100.00 24.00 50.10 25.90

208 - 218 B -213 -218 15.45 83.68 0.65 0.22 100.00 98.98 0.77 0.26

218 - 228 A -218 -223 4.01 93.64 2.03 0.32 100.00 97.55 2.12 0.33

218 - 228 B -223 -228 19.73 78.04 1.97 0.27 100.00 97.21 2.45 0.34

228 - 238 A -228 -233 9.63 85.56 4.07 0.75 100.00 94.67 4.50 0.83

228 - 238 B -233 -238 1.93 88.84 7.76 1.47 100.00 90.59 7.91 1.50

238 - 248 A -238 -243 1.91 95.89 1.90 0.30 100.00 97.76 1.94 0.30

238 - 248 B -243 -248 21.71 73.83 3.74 0.72 100.00 94.30 4.77 0.92

248 - 259 A -248 -254 58.40 37.63 3.28 0.68 100.00 90.47 7.88 1.64

248 - 259 B -254 -259 48.81 45.95 4.29 0.95 100.00 89.78 8.37 1.85



100

Tota

l W

eig

ht

Sam

ple

ID

5 (φ

= -

2)10

(φ

= -

1)18

(φ

= 0

)35

(φ

= 1

)60

(φ

= 2

)12

0 (φ

= 3

)23

0 (φ

= 4

)Si

lt (

φ ≥

5)

Cla

y (φ

≥ 5

)(G

ram

s)

9 -

19 A

-1-9

.00

-10.

3132

.05

12.7

536

.27

57.0

310

3.94

79.4

935

.04

33.6

110

.66

400.

84

9 -

19 A

-2-1

0.31

-12.

2841

.08

14.4

729

.00

51.6

799

.08

76.6

435

.64

43.3

39.

7640

0.67

9 -

19 A

-3-1

2.28

-14.

0042

.44

17.5

836

.36

60.4

310

0.22

67.3

330

.69

36.2

19.

5440

0.80

9 -

19 B

-14.

00-1

9.00

22.1

324

.77

47.2

556

.57

92.2

173

.31

37.9

635

.53

11.4

040

1.13

19 -

26

A-1

-19.

00-1

9.94

1.78

9.41

30.4

386

.02

165.

2481

.41

16.5

28.

731.

3640

0.90

19 -

26

A-2

-19.

94-2

2.50

41.0

915

.00

16.6

728

.53

84.0

884

.68

41.1

410

9.59

29.7

045

0.48

19 -

26

B-1

-22.

50-2

3.42

24.1

414

.23

15.3

227

.57

85.5

795

.71

54.5

612

7.39

33.9

847

8.47

19 -

26

B-2

-23.

42-2

4.33

23.6

234

.60

60.0

373

.03

95.0

943

.98

21.0

642

.15

7.32

400.

88

19 -

26

B-3

-24.

33-2

6.00

56.0

231

.45

41.1

775

.65

146.

2234

.60

7.86

6.68

0.84

400.

49

26 -

29

A-1

-26.

00-2

7.01

28.7

314

.17

15.1

634

.16

90.9

466

.33

60.4

511

9.01

21.7

345

0.68

26 -

29

A-2

-27.

01-2

9.00

0.26

1.20

1.44

24.2

029

8.61

70.4

43.

091.

260.

1440

0.64

29 -

36

A-1

-29.

00-3

0.17

28.5

114

.61

27.4

162

.24

121.

8711

2.65

23.8

98.

311.

1940

0.68

29 -

36

A-2

-30.

17-3

0.24

87.0

219

.22

15.8

625

.35

68.9

189

.03

45.0

381

.30

18.0

344

9.75

29 -

36

A-3

-30.

24-3

2.50

61.1

032

.39

33.6

043

.00

86.8

495

.99

31.3

814

.44

1.69

400.

43

29 -

36

B-1

-32.

50-3

3.90

5.66

5.10

10.0

425

.05

80.5

476

.44

108.

7612

3.40

15.0

845

0.07

29 -

36

B-2

-33.

90-3

6.00

40.9

99.

9812

.67

20.5

356

.78

55.6

639

.59

186.

0327

.64

449.

87

36 -

39

A-1

-36.

00-3

7.05

31.0

214

.25

15.4

630

.08

107.

2889

.59

42.1

912

6.13

19.2

047

5.20

36 -

39

A-2

-37.

05-3

9.00

35.8

715

.68

14.9

824

.67

104.

1311

4.54

43.9

044

.67

2.34

400.

78

39 -

49

A-1

-39.

00-4

1.27

40.1

034

.02

42.2

074

.95

151.

4624

.82

8.53

21.2

43.

5140

0.83

39 -

49

A-2

-41.

27-4

2.43

127.

5033

.22

32.0

648

.15

73.0

934

.39

22.6

623

.24

6.05

400.

36

39 -

49

A-3

-42.

43-4

4.00

75.3

528

.42

36.7

471

.71

108.

0439

.32

16.6

720

.29

4.09

400.

63

39 -

49

B-1

-44.

00-4

6.27

83.9

524

.19

30.0

764

.20

119.

8633

.63

14.7

326

.09

3.82

400.

54

39 -

49

B-2

-46.

27-4

9.00

10.1

86.

429.

5626

.97

155.

8511

0.91

47.1

828

.47

4.96

400.

50

49 -

59

A-4

9.00

-54.

0088

.46

24.0

126

.04

58.6

012

0.11

47.0

613

.55

19.5

93.

1940

0.61

49 -

59

B-5

4.00

-59.

0046

.29

40.8

547

.91

73.3

414

3.28

24.4

48.

0614

.41

2.10

400.

68

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

KA

-13-

01 S

ampl

e M

asse

s

101

Tota

l W

eig

ht

Sam

ple

ID

5 (φ

= -

2)10

(φ

= -

1)18

(φ

= 0

)35

(φ

= 1

)60

(φ

= 2

)12

0 (φ

= 3

)23

0 (φ

= 4

)Si

lt (

φ ≥

5)

Cla

y (φ

≥ 5

)(G

ram

s)

59 -

69

A-1

-59.

00-6

1.50

53.3

723

.80

35.7

682

.49

152.

2232

.44

7.09

11.8

41.

6840

0.69

59 -

69

A-2

-61.

50-6

4.00

125.

7957

.56

47.8

458

.41

75.4

418

.93

5.90

9.35

1.32

400.

54

59 -

69

B-6

4.00

-69.

0071

.07

25.5

725

.73

42.5

714

6.17

69.3

810

.40

8.52

1.16

400.

57

69 -

79

A-6

9.00

-74.

0029

.68

19.7

527

.89

84.7

518

2.32

46.9

74.

784.

170.

5540

0.86

69 -

79

B-7

4.00

-79.

0081

.91

33.7

037

.06

67.6

112

5.19

38.1

46.

848.

981.

2240

0.65

79 -

89

A-7

9.00

-84.

7042

.34

14.3

327

.20

71.7

815

5.05

68.8

410

.24

9.23

1.85

400.

86

79 -

89

B-8

4.70

-89.

000.

794.

8311

.77

56.1

022

8.71

80.8

110

.58

6.21

0.79

400.

59

89 -

99

A-8

9.00

-94.

0070

.85

25.1

533

.24

66.1

014

1.36

43.2

19.

3310

.02

1.30

400.

56

89 -

99

B-1

-94.

00-9

6.51

2.27

2.47

6.90

43.1

520

7.20

116.

7314

.62

6.53

0.65

400.

52

89 -

99

B-2

-96.

51-9

9.00

23.0

327

.63

37.2

947

.41

151.

0996

.32

8.36

8.12

1.10

400.

35

99 -

109

A-9

9.00

-104

.00

0.08

1.68

6.97

49.4

024

7.32

76.1

77.

6710

.09

1.23

400.

61

99 -

109

B-1

-104

.00

-106

.52

0.33

1.92

4.21

25.0

323

5.07

111.

229.

1311

.84

1.73

400.

48

99 -

109

B-2

-106

.52

-109

.00

13.3

030

.01

80.4

413

6.27

94.8

022

.32

7.01

13.7

42.

4740

0.36

109

- 11

9 A

-109

.00

-113

.34

0.21

0.11

0.18

1.70

141.

3323

9.56

12.7

64.

180.

5640

0.59

109

- 11

9 B

-113

.34

-119

.00

72.1

539

.21

60.2

592

.68

76.7

732

.02

10.3

314

.35

2.63

400.

39

119

- 12

9 A

-1-1

19.0

0-1

21.2

638

.76

21.4

338

.50

131.

6312

5.89

29.5

35.

588.

071.

3340

0.72

119

- 12

9 A

-2-1

21.2

6-1

24.0

00.

602.

515.

5210

.04

67.6

929

8.87

10.1

64.

700.

5440

0.63

119

- 12

9 B

-124

.00

-129

.00

0.00

0.12

0.60

11.1

319

9.90

172.

368.

317.

081.

0540

0.55

129

- 13

9 A

-1-1

29.0

0-1

30.1

514

7.16

46.0

129

.04

47.8

768

.97

35.3

912

.19

11.0

32.

8640

0.52

129

- 13

9 A

-2-1

30.1

5-1

34.0

013

.17

7.34

8.89

19.6

475

.66

97.7

055

.27

135.

0638

.49

451.

22

129

- 13

9 B

-1-1

34.0

0-1

35.1

68.

376.

488.

4018

.74

77.2

710

5.45

63.8

912

5.32

69.3

748

3.29

129

- 13

9 B

-2-1

35.1

6-1

39.0

01.

512.

283.

7014

.72

123.

9917

4.49

68.0

211

.10

0.84

400.

65

139

- 14

9 A

-139

.00

-144

.00

0.33

0.41

1.31

9.53

87.1

318

1.75

91.2

125

.64

3.07

400.

38

139

- 14

9 B

-1-1

44.0

0-1

46.3

30.

000.

020.

292.

7257

.12

177.

4912

6.00

31.6

43.

6239

8.90

139

- 14

9 B

-2-1

46.3

3-1

49.0

02.

221.

733.

1411

.43

101.

0316

9.00

54.1

826

.19

3.33

372.

25

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

KA

-13-

01 S

ampl

e M

asse

s

102

Sam

ple

ID

5 (φ

= -

2 )

10 (

φ =

-1)

18 (

φ =

0)

35 (

φ =

1)

60 (

φ =

2)

120

(φ =

3)

230

(φ =

4)

Silt

(φ

≥ 5

)Cl

ay

(φ ≥

5)

Sam

ple

To

tal

(%)

9 -

19 A

-1-9

.00

-10.

318.

003.

189.

0514

.23

25.9

319

.83

8.74

88.9

68.

392.

6610

0.00

9 -

19 A

-2-1

0.31

-12.

2810

.25

3.61

7.24

12.9

024

.73

19.1

38.

9086

.75

10.8

12.

4410

0.00

9 -

19 A

-3-1

2.28

-14.

0010

.59

4.39

9.07

15.0

825

.00

16.8

07.

6688

.59

9.03

2.38

100.

00

9 -

19 B

-14.

00-1

9.00

5.52

6.18

11.7

814

.10

22.9

918

.28

9.46

88.3

08.

862.

8410

0.00

19 -

26

A-1

-19.

00-1

9.94

0.44

2.35

7.59

21.4

641

.22

20.3

14.

1297

.48

2.18

0.34

100.

00

19 -

26

A-2

-19.

94-2

2.50

9.12

3.33

3.70

6.33

18.6

618

.80

9.13

69.0

824

.33

6.59

100.

00

19 -

26

B-1

-22.

50-2

3.42

5.05

2.97

3.20

5.76

17.8

820

.00

11.4

066

.27

26.6

27.

1010

0.00

19 -

26

B-2

-23.

42-2

4.33

5.89

8.63

14.9

718

.22

23.7

210

.97

5.25

87.6

610

.51

1.83

100.

00

19 -

26

B-3

-24.

33-2

6.00

13.9

97.

8510

.28

18.8

936

.51

8.64

1.96

98.1

21.

670.

2110

0.00

26 -

29

A-1

-26.

00-2

7.01

6.37

3.14

3.36

7.58

20.1

814

.72

13.4

168

.77

26.4

14.

8210

0.00

26 -

29

A-2

-27.

01-2

9.00

0.06

0.30

0.36

6.04

74.5

317

.58

0.77

99.6

50.

310.

0410

0.00

29 -

36

A-1

-29.

00-3

0.17

7.12

3.65

6.84

15.5

330

.42

28.1

15.

9697

.63

2.07

0.30

100.

00

29 -

36

A-2

-30.

17-3

0.24

19.3

54.

273.

535.

6415

.32

19.8

010

.01

77.9

118

.08

4.01

100.

00

29 -

36

A-3

-30.

24-3

2.50

15.2

68.

098.

3910

.74

21.6

923

.97

7.84

95.9

73.

610.

4210

0.00

29 -

36

B-1

-32.

50-3

3.90

1.26

1.13

2.23

5.57

17.8

916

.98

24.1

769

.23

27.4

23.

3510

0.00

29 -

36

B-2

-33.

90-3

6.00

9.11

2.22

2.82

4.56

12.6

212

.37

8.80

52.5

041

.35

6.14

100.

00

36 -

39

A-1

-36.

00-3

7.05

6.53

3.00

3.25

6.33

22.5

818

.85

8.88

69.4

226

.54

4.04

100.

00

36 -

39

A-2

-37.

05-3

9.00

8.95

3.91

3.74

6.16

25.9

828

.58

10.9

588

.27

11.1

50.

5810

0.00

39 -

49

A-1

-39.

00-4

1.27

10.0

08.

4910

.53

18.7

037

.79

6.19

2.13

93.8

35.

300.

8810

0.00

39 -

49

A-2

-41.

27-4

2.43

31.8

58.

308.

0112

.03

18.2

68.

595.

6692

.68

5.81

1.51

100.

00

39 -

49

A-3

-42.

43-4

4.00

18.8

17.

099.

1717

.90

26.9

79.

814.

1693

.91

5.06

1.02

100.

00

39 -

49

B-1

-44.

00-4

6.27

20.9

66.

047.

5116

.03

29.9

28.

403.

6892

.53

6.51

0.95

100.

00

39 -

49

B-2

-46.

27-4

9.00

2.54

1.60

2.39

6.73

38.9

127

.69

11.7

891

.65

7.11

1.24

100.

00

49 -

59

A-4

9.00

-54.

0022

.08

5.99

6.50

14.6

329

.98

11.7

53.

3894

.31

4.89

0.80

100.

00

49 -

59

B-5

4.00

-59.

0011

.55

10.2

011

.96

18.3

035

.76

6.10

2.01

95.8

83.

600.

5210

0.00

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

Gra

vel

& S

an

d

Tota

l (%

)

KA

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01 S

ampl

e W

eigh

t Pe

rcen

ts

103

Sam

ple

ID

5 (φ

= -

2 )

10 (

φ =

-1)

18 (

φ =

0)

35 (

φ =

1)

60 (

φ =

2)

120

(φ =

3)

230

(φ =

4)

Silt

(φ

≥ 5

)Cl

ay

(φ ≥

5)

Sam

ple

To

tal

(%)

59 -

69

A-1

-59.

00-6

1.50

13.3

25.

948.

9220

.59

37.9

98.

101.

7796

.63

2.96

0.42

100.

00

59 -

69

A-2

-61.

50-6

4.00

31.4

114

.37

11.9

414

.58

18.8

34.

731.

4797

.34

2.33

0.33

100.

00

59 -

69

B-6

4.00

-69.

0017

.74

6.38

6.42

10.6

336

.49

17.3

22.

6097

.58

2.13

0.29

100.

00

69 -

79

A-6

9.00

-74.

007.

404.

936.

9621

.14

45.4

811

.72

1.19

98.8

21.

040.

1410

0.00

69 -

79

B-7

4.00

-79.

0020

.44

8.41

9.25

16.8

831

.25

9.52

1.71

97.4

52.

240.

3110

0.00

79 -

89

A-7

9.00

-84.

7010

.56

3.57

6.79

17.9

138

.68

17.1

72.

5597

.24

2.30

0.46

100.

00

79 -

89

B-8

4.70

-89.

000.

201.

212.

9414

.00

57.0

920

.17

2.64

98.2

51.

550.

2010

0.00

89 -

99

A-8

9.00

-94.

0017

.69

6.28

8.30

16.5

035

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10.7

92.

3397

.17

2.50

0.33

100.

00

89 -

99

B-1

-94.

00-9

6.51

0.57

0.62

1.72

10.7

751

.73

29.1

43.

6598

.21

1.63

0.16

100.

00

89 -

99

B-2

-96.

51-9

9.00

5.75

6.90

9.31

11.8

437

.74

24.0

62.

0997

.70

2.03

0.27

100.

00

99 -

109

A-9

9.00

-104

.00

0.02

0.42

1.74

12.3

361

.74

19.0

11.

9197

.17

2.52

0.31

100.

00

99 -

109

B-1

-104

.00

-106

.52

0.08

0.48

1.05

6.25

58.7

027

.77

2.28

96.6

12.

960.

4310

0.00

99 -

109

B-2

-106

.52

-109

.00

3.32

7.50

20.0

934

.04

23.6

85.

571.

7595

.95

3.43

0.62

100.

00

109

- 11

9 A

-109

.00

-113

.34

0.05

0.03

0.04

0.42

35.2

859

.80

3.19

98.8

21.

040.

1410

0.00

109

- 11

9 B

-113

.34

-119

.00

18.0

29.

7915

.05

23.1

519

.17

8.00

2.58

95.7

63.

580.

6610

0.00

119

- 12

9 A

-1-1

19.0

0-1

21.2

69.

675.

359.

6132

.85

31.4

27.

371.

3997

.65

2.01

0.33

100.

00

119

- 12

9 A

-2-1

21.2

6-1

24.0

00.

150.

631.

382.

5116

.90

74.6

02.

5498

.69

1.17

0.14

100.

00

119

- 12

9 B

-124

.00

-129

.00

0.00

0.03

0.15

2.78

49.9

143

.03

2.07

97.9

71.

770.

2610

0.00

129

- 13

9 A

-1-1

29.0

0-1

30.1

536

.74

11.4

97.

2511

.95

17.2

28.

843.

0496

.53

2.75

0.72

100.

00

129

- 13

9 A

-2-1

30.1

5-1

34.0

02.

921.

631.

974.

3516

.77

21.6

512

.25

61.5

429

.93

8.53

100.

00

129

- 13

9 B

-1-1

34.0

0-1

35.1

61.

731.

341.

743.

8815

.99

21.8

213

.22

59.7

225

.93

14.3

510

0.00

129

- 13

9 B

-2-1

35.1

6-1

39.0

00.

380.

570.

923.

6730

.95

43.5

516

.98

97.0

22.

770.

2110

0.00

139

- 14

9 A

-139

.00

-144

.00

0.08

0.10

0.33

2.38

21.7

645

.39

22.7

892

.83

6.40

0.77

100.

00

139

- 14

9 B

-1-1

44.0

0-1

46.3

30.

000.

010.

070.

6814

.32

44.4

931

.59

91.1

67.

930.

9110

0.00

139

- 14

9 B

-2-1

46.3

3-1

49.0

00.

600.

460.

843.

0727

.14

45.4

014

.55

92.0

77.

040.

8910

0.00

De

pth

(fe

et

fro

m s

urf

ace

)

Pan

(p

hi

Va

lue

)Si

eve

Nu

mb

er

(ph

i V

alu

e)

Gra

vel

& S

an

d

Tota

l (%

)

KA

-13-

01 S

ampl

e W

eigh

t Pe

rcen

ts

104


9 - 19 A-1 -9.00 -10.31 11.18 77.78 8.39 2.66 100.00 87.57 9.44 2.99

9 - 19 A-2 -10.31 -12.28 13.86 72.89 10.81 2.44 100.00 84.62 12.55 2.83

9 - 19 A-3 -12.28 -14.00 14.98 73.61 9.03 2.38 100.00 86.57 10.62 2.80

9 - 19 B -14.00 -19.00 11.69 76.61 8.86 2.84 100.00 86.75 10.03 3.22

19 - 26 A-1 -19.00 -19.94 2.79 94.69 2.18 0.34 100.00 97.41 2.24 0.35

19 - 26 A-2 -19.94 -22.50 12.45 56.63 24.33 6.59 100.00 64.68 27.79 7.53

19 - 26 B-1 -22.50 -23.42 8.02 58.25 26.62 7.10 100.00 63.33 28.95 7.72

19 - 26 B-2 -23.42 -24.33 14.52 73.14 10.51 1.83 100.00 85.56 12.30 2.14

19 - 26 B-3 -24.33 -26.00 21.84 76.28 1.67 0.21 100.00 97.60 2.13 0.27

26 - 29 A-1 -26.00 -27.01 9.52 59.25 26.41 4.82 100.00 65.49 29.18 5.33

26 - 29 A-2 -27.01 -29.00 0.36 99.29 0.31 0.04 100.00 99.65 0.31 0.04

29 - 36 A-1 -29.00 -30.17 10.76 86.87 2.07 0.30 100.00 97.34 2.33 0.33

29 - 36 A-2 -30.17 -30.24 23.62 54.29 18.08 4.01 100.00 71.08 23.67 5.25

29 - 36 A-3 -30.24 -32.50 23.35 72.62 3.61 0.42 100.00 94.74 4.70 0.55

29 - 36 B-1 -32.50 -33.90 2.39 66.84 27.42 3.35 100.00 68.48 28.09 3.43

29 - 36 B-2 -33.90 -36.00 11.33 41.17 41.35 6.14 100.00 46.44 46.64 6.93

36 - 39 A-1 -36.00 -37.05 9.53 59.89 26.54 4.04 100.00 66.20 29.34 4.47

36 - 39 A-2 -37.05 -39.00 12.86 75.41 11.15 0.58 100.00 86.54 12.79 0.67

39 - 49 A-1 -39.00 -41.27 18.49 75.33 5.30 0.88 100.00 92.42 6.50 1.07

39 - 49 A-2 -41.27 -42.43 40.14 52.54 5.81 1.51 100.00 87.78 9.70 2.52

39 - 49 A-3 -42.43 -44.00 25.90 68.01 5.06 1.02 100.00 91.79 6.83 1.38

39 - 49 B-1 -44.00 -46.27 27.00 65.53 6.51 0.95 100.00 89.77 8.92 1.31

39 - 49 B-2 -46.27 -49.00 4.14 87.51 7.11 1.24 100.00 91.29 7.42 1.29

49 - 59 A -49.00 -54.00 28.07 66.24 4.89 0.80 100.00 92.09 6.80 1.11

49 - 59 B -54.00 -59.00 21.75 74.13 3.60 0.52 100.00 94.73 4.60 0.67

59 - 69 A-1 -59.00 -61.50 19.26 77.37 2.96 0.42 100.00 95.82 3.66 0.52

59 - 69 A-2 -61.50 -64.00 45.78 51.56 2.33 0.33 100.00 95.09 4.30 0.61

59 - 69 B -64.00 -69.00 24.13 73.46 2.13 0.29 100.00 96.82 2.80 0.38

69 - 79 A -69.00 -74.00 12.33 86.49 1.04 0.14 100.00 98.66 1.19 0.16

69 - 79 B -74.00 -79.00 28.86 68.60 2.24 0.31 100.00 96.42 3.15 0.43

79 - 89 A -79.00 -84.70 14.14 83.10 2.30 0.46 100.00 96.78 2.68 0.54

79 - 89 B -84.70 -89.00 1.40 96.85 1.55 0.20 100.00 98.23 1.57 0.20

89 - 99 A -89.00 -94.00 23.97 73.21 2.50 0.33 100.00 96.28 3.29 0.43

89 - 99 B-1 -94.00 -96.51 1.18 97.02 1.63 0.16 100.00 98.19 1.65 0.16

89 - 99 B-2 -96.51 -99.00 12.65 85.04 2.03 0.27 100.00 97.36 2.32 0.31

99 - 109 A -99.00 -104.00 0.44 96.73 2.52 0.31 100.00 97.16 2.53 0.31

99 - 109 B-1 -104.00 -106.52 0.56 96.05 2.96 0.43 100.00 96.59 2.97 0.43

99 - 109 B-2 -106.52 -109.00 10.82 85.13 3.43 0.62 100.00 95.46 3.85 0.69

109 - 119 A -109.00 -113.34 0.08 98.74 1.04 0.14 100.00 98.82 1.04 0.14

109 - 119 B -113.34 -119.00 27.81 67.95 3.58 0.66 100.00 94.13 4.96 0.91

119 - 129 A-1 -119.00 -121.26 15.02 82.63 2.01 0.33 100.00 97.24 2.37 0.39

119 - 129 A-2 -121.26 -124.00 0.78 97.92 1.17 0.14 100.00 98.68 1.18 0.14

119 - 129 B -124.00 -129.00 0.03 97.94 1.77 0.26 100.00 97.97 1.77 0.26

129 - 139 A-1 -129.00 -130.15 48.23 48.30 2.75 0.72 100.00 93.30 5.32 1.38

129 - 139 A-2 -130.15 -134.00 4.55 56.99 29.93 8.53 100.00 59.71 31.36 8.94

129 - 139 B-1 -134.00 -135.16 3.07 56.64 25.93 14.35 100.00 58.44 26.75 14.81

129 - 139 B-2 -135.16 -139.00 0.95 96.07 2.77 0.21 100.00 96.99 2.80 0.21

139 - 149 A -139.00 -144.00 0.18 92.64 6.40 0.77 100.00 92.82 6.42 0.77

139 - 149 B-1 -144.00 -146.33 0.01 91.16 7.93 0.91 100.00 91.16 7.93 0.91

139 - 149 B-2 -146.33 -149.00 1.06 91.01 7.04 0.89 100.00 91.98 7.11 0.90



105

APPENDIX B

Atterberg Limits Results

106

Sample(ft) 64.17

wt (g) 146.15

Plastic Limit

B-1 B-2

13.98 12.85

13.66 12.64

11.12 11.05 Average

12.60 13.21 12.90

Liquid Limit

B-3 B-4

23.00 21.94

21.07 20.17

11.10 11.09

19.36 19.49

29 28 Average

19.71 19.76 19.74

20

13

7

NOTE:

Core BA-09-02

LL, ASTM Single Point

LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)

PLASTICITY INDEX (PI)

Container No.

Mass Moist Soil+Container, M1 (g)

Mass Dry Soil+Container, M2 (g)

Mass Container, M3 (g)

Water Content (w) (%)

Number of Blows (N)

Container No.





107

Sample(ft) 72.58

wt (g) 148.67

Plastic Limit

B-5 B-6

13.21 13.05

12.98 12.80

11.12 10.83 Average

12.37 12.69 12.53

Liquid Limit

B-7 B-8

20.97 22.83

19.11 20.64

11.12 11.09

23.28 22.93

30 28 Average

23.80 23.25 23.52

24

13

11

NOTE:

Core BA-09-02


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)


Container No.





Number of Blows (N)

Container No.





108

Sample(ft) 126

wt (g) 132.32

Plastic Limit

B-9 B-10

12.86 13.24

12.64 12.96

11.12 11.05 Average

14.47 14.66 14.57

Liquid Limit

B-11 B-12

22.49 23.19

19.95 20.54

11.07 11.09

28.60 28.04

29 30 Average

29.12 28.67 28.89

29

15

14

NOTE:

Core BA-09-02




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)



Container No.



Container No.



109

Sample(ft) 138

wt (g) 159.82

Plastic Limit

B-13 B-14

12.95 12.54

12.68 12.35

10.82 11.06 Average

14.52 14.73 14.62

Liquid Limit

B-15 B-16

21.76 23.09

19.20 20.19

11.11 11.07

31.64 31.80

30 30 Average

32.35 32.51 32.43

32

15

18

NOTE:

Core BA-09-02




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


110

Sample(ft) 152.25

wt (g) 145.70

Plastic Limit

B-17 B-18

14.18 14.16

13.82 13.80

11.05 11.08 Average

13.00 13.24 13.12

Liquid Limit

B-19 B-20

21.64 21.89

19.25 19.38

11.20 10.96

29.69 29.81

27 26 Average

29.97 29.95 29.96

30

13

17

NOTE:

Core BA-09-02




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


111

Sample(ft) 183

wt (g) 155.41

Plastic Limit

B-21 B-22

13.21 13.36

13.00 13.11

11.10 10.82 Average

11.05 10.92 10.98

Liquid Limit

B-23 B-24

23.41 22.66

21.41 20.80

10.91 11.07

19.05 19.12

25 27 Average

19.05 19.29 19.17

19

11

8

NOTE:

Core BA-09-02




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


112

Sample(ft) 31.75

wt (g) 130.08

Plastic Limit

C-1 C-2

14.33 14.29

14.04 14.00

10.82 10.82 Average

9.01 9.12 9.06

Liquid Limit

C-3 C-4

22.23 23.92

20.59 22.05

11.08 11.15

17.25 17.16

21 21 Average

16.89 16.80 16.84

17

9

8

NOTE:

Core BA-10-02




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


113

Sample(ft) 37.75

wt (g) 134.36

Plastic Limit

C-5 C-6

13.12 13.32

12.93 13.11

11.07 11.12 Average

10.22 10.55 10.38

Liquid Limit

C-7 C-8

24.53 25.56

22.80 23.74

10.92 11.12

14.56 14.42

23 23 Average

14.42 14.28 14.35

14

10

4

NOTE:

Core BA-10-02




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


114

Sample(ft) 93.58

wt (g) 134.36

Plastic Limit

C-9 C-10

12.91 12.58

12.75 12.42

11.33 11.04 Average

11.27 11.59 11.43

Liquid Limit

C-11 C-12

23.66 23.33

22.04 21.78

10.96 11.20

14.62 14.65

21 23 Average

14.32 14.50 14.41

14

11

3

NOTE:




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


Core BA-10-02

115

Sample(ft) 103.42

wt (g) 124.62

Plastic Limit

C-13 C-14

12.38 12.89

12.23 12.69

10.97 11.03 Average

11.90 12.05 11.98

Liquid Limit

C-15 C-16

22.52 21.52

21.02 20.19

10.91 11.32

14.84 14.99

22 20 Average

14.61 14.59 14.60

15

12

3

NOTE:




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


Core BA-10-02

116

Sample(ft) 181.25

wt (g) 158.19

Plastic Limit

C-17 C-18

15.26 14.78

14.85 14.39

11.20 10.99 Average

11.23 11.47 11.35

Liquid Limit

C-19 C-20

22.74 22.30

20.82 20.47

11.11 11.09

19.77 19.51

22 23 Average

19.47 19.31 19.39

19

11

8

NOTE:




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


Core BA-10-02

117

Sample(ft) 235.25

wt (g) 148.08

Plastic Limit

C-21 C-22

13.85 13.03

13.53 12.80

11.08 11.04 Average

13.06 13.07 13.06

Liquid Limit

C-23 C-24

24.39 21.81

22.30 20.12

11.12 11.06

18.69 18.65

24 23 Average

18.60 18.47 18.53

19

13

5

NOTE:




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


Core BA-10-02

118

Sample(ft) 239.7

wt (g) 138.60

Plastic Limit

C-25 C-26

12.92 13.68

12.57 13.26

10.83 11.13 Average

20.11 19.72 19.92

Liquid Limit

C-27 C-28

21.59 21.47

18.60 18.54

10.93 11.05

38.98 39.12

29 29 Average

39.69 39.83 39.76

40

20

20

NOTE:




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)




Container No.



Container No.


Core BA-10-02

119

Sample (ft) 30

wt (g) 130.04

Plastic Limit

E-1 E-2

14.87 14.93

14.44 14.52

10.82 11.07 Average

11.88 11.88 11.88

Liquid Limit

E-3 E-4

24.40 24.72

22.67 22.91

11.17 11.02

15.04 15.22

23 22 Average

14.89 14.99 14.94

15

12

3

NOTE:



Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)


Container No.





Container No.



Core CA-11-01

120

Sample (ft) 50

wt (g) 134.54

Plastic Limit

E-5 E-6

14.41 14.21

14.09 13.85

11.12 11.07 Average

10.77 12.95 11.86

Liquid Limit

E-7 E-8

23.05 21.56

21.41 20.11

10.97 11.02

15.71 15.95

24 23 Average

15.63 15.79 15.71

16

12

4

NOTE:



Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)


Container No.





Container No.



Core CA-11-01

121

Sample (ft) 72

wt (g) 150.68

Plastic Limit

E-9 E-10

14.69 14.31

14.29 13.96

10.91 11.13 Average

11.83 12.37 12.10

Liquid Limit

E-11 E-12

22.22 23.10

20.78 21.58

11.06 11.03

14.81 14.41

22 22 Average

14.59 14.19 14.39

14

12

2

NOTE:




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)


Container No.





Container No.


Core CA-11-01

122

Sample (ft) 83

wt (g) 153.92

Plastic Limit

E-13 E-14

14.52 14.76

14.14 14.36

11.11 11.08 Average

12.54 12.20 12.37

Liquid Limit

E-15 E-16

23.16 21.53

21.61 20.19

10.99 11.03

14.60 14.63

22 22 Average

14.37 14.40 14.39

14

12

2

NOTE:

Core CA-11-01




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)


Container No.





Container No.


123

Sample (ft) 150

wt (g) 135.1

Plastic Limit

E-13 E-14

13.54 13.93

13.24 13.61

10.90 11.05 Average

12.82 12.50 12.66

Liquid Limit

E-15 E-16

23.22 23.71

21.19 21.57

11.34 11.05

20.61 20.34

20 21 Average

20.06 19.92 19.99

20

13

7

NOTE:

Core CA-11-01




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)


Container No.





Container No.


124

Sample (ft) 155

wt (g) 134.5

Plastic Limit

E-13 E-14

13.59 13.29

13.26 12.99

11.13 11.07 Average

15.49 15.62 15.56

Liquid Limit

E-15 E-16

22.12 22.09

19.85 19.86

10.98 11.03

25.59 25.25

22 23 Average

25.20 25.00 25.10

25

16

10

NOTE:

Core CA-11-01




Number of Blows (N)


LIQUID LIMIT (LL)

PLASTIC LIMIT (PL)


Container No.





Container No.


125

APPENDIX C

Bulk Organic Carbon Results

126

Eq. 0

.64

32

(x)

– 2

.44

02

, R2 =

0.9

92

De

pth

We

igh

tC

O2

Pre

ssu

reC

O2

CO

2O

C

(ft)

(mg)

(mm

Hg)

(nm

ol)

(mg)

(%)

BA

-09-

01A

-118

060

2.20

173.

3010

9.03

1.30

80.

217

BA

-09-

01A

-319

451

2.80

131.

9090

.30

1.08

40.

211

BA

-09-

02B

-164

631.

3028

6.50

181.

842.

182

0.34

6

BA

-09-

02B

-272

606.

8038

1.10

242.

682.

912

0.48

0

BA

-09-

02B

-515

250

6.60

305.

5019

4.06

2.32

90.

460

BA

-10-

02C

-132

513.

6032

4.80

206.

472.

478

0.47

6

BA

-10-

02C

-394

709.

9011

3.50

70.5

60.

847

0.18

5

BA

-10-

02C

-618

612

08.0

013

4.70

84.2

01.

010

0.10

1

BA

-10-

02C

-723

551

7.40

219.

6013

8.81

1.66

60.

322

CA

-11-

01E-

131

1183

.90

165.

4010

3.95

1.24

70.

093

CA

-11-

01E-

371

502.

9021

5.40

136.

111.

633

0.32

5

CA

-11-

01E-

615

150

9.70

508.

8032

4.82

3.89

80.

765

OT-

12-0

1F-

131

509.

3035

6.30

226.

732.

721

0.53

4

OT-

12-0

1F-

296

502.

4017

2.80

108.

711.

305

0.26

0

Co

re ID

Sam

ple

ID

CO

2 A

nal

ysis

127

APPENDIX D

δ13

C Results

128

Depth

(ft)

BA-09-01 A-1 180 -25.929

BA-09-01 A-3 194 -26.001

BA-09-02 B-1 64 -25.408

BA-09-02 B-2 72 -26.192

BA-09-02 B-5 152 -25.5

BA-10-02 C-1 32 -25.913

BA-10-02 C-3 94 -26.045

BA-10-02 C-6 186 -23.533

BA-10-02 C-7 235 -24.201

CA-11-01 E-1 31 -25.203

CA-11-01 E-3 71 -24.957

CA-11-01 E-6 151 -25.943

OT-12-01 F-1 31 -25.422

OT-12-01 F-2 96 -26.529

Core ID Sample ID δ13

C

Stable Isotope Analysis

129

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