Z8April 198.5 - DTIC

ST. LOUIS DISTRICT . LTURALRESOURCEMANAGEMENTREV)RT UMBER 17

AD-A2 4 5 724

SHALLOW SUBSURFACE GEOLOGY, GEOMORPHOLOGY ANDLIMITED CULTURAL RESOURCE INVESTIGATIONS OF THEMEREDOSIA VILLAGE A AND MEREDOSIA LAKE LEVEE ANDDRAINAGE DISTRICTS, SCOTT, MORGAN, AND CASSCOUNTIES ILLINOIS

Contract No. DACW43-82-D-O083

by Edwin R. Hajic and David S. Leigh

Harold Hassen, Principal Invesiiigator, DTACCenter for American Archeolox l E LEO32C Tr

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BESTAVAILABLE ....

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IUJS Arliy CorpsI I ' i Iof Engineers

* 9. ~31 Z8April 198.5

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BEFORE COMPLETING FORM1. REPORT NUMBER 2. GOVT ACCESSION NO. 3. RECIPIENT'S CATALOG NUMBER

4. TITLE (anud Subtle) SALW UTURFACL GEOLOGY, 5. TYPE OF REPORT & PERIOD COVEREDGEOMORPHOLOGY AND LIMITED CULTURAL RESOURCE

INVESTIGATIONS OF THE MEREDOSIA VILLAGE ANDMEREDOSIA LAKE LEVEE AND DRAINAGE DISTRICTS, 6. PERFORMING ORG. REPORT NUMBERSCOTT, MORGAN, AND CASS COUNTIES, ILLINOIS. SLD CRM REPORT 17

7. AUTHOR(e) 8. CONTRACT OR GRANT NUMBER(a)

Edwin R. Hajic and David S. Leigh DACW43-82-D-0083

9 PERFORMNG ORGAN17ATION NAME AI ADDRESS 10. PROGRAM ELEMENT. PROJECT, TASKenter. for Amezc~n A'c e8ov AREA & WORK UNIT NUMBERSiampsv le^Arcneo -g al enor

P.O. Box 20

Kampsville, IL 62053

I. CONTROLLING OFFICE NAME AND ADDRESS 12. REPORT DATE

U.S. ARMY ENGINEER DISTRICT, ST. LOUIS April 1985

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- The Meredosia Village and Meredosia Lake Levee and Drainage District study isthe fifth of an ongoing series of combined geologic, geomorphic, andarcheological surveys of lower Illinois River valley levee and drainagedistricts. Subsurface investigations in Illinois Valley deposits are used inconcert with geomorphic analysis and radiocarbon dates to identify, spatiallydelimit and date lithostratigraphic units, interpret depositionalenvironments, and reconstruct the terminal Wisconsinan and Holocene valley - --

DO ,o" 1473 OMroN oF t oV 5OkOLETI1 AN7 SEC¢UmrvYCLAI~t PICA'rOW OF "rhtl'"At .....es nt~d

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evolution. Within this contextual framework, evaluations of the location andpreservation potentials for surface and buried archeological sites are made.

SECURITY CLASSIFICATION OF THIS PAGE(W7en Date Entered)

ST. LOUIS DISTRICT CULTURAL RESOURCE MANAGEMENT REPORT NUMBER 17

Shallow Subsurface Geology, Geomorphology and Limited Cultural Resource

Investigations of the Meredosia Village and Meredosia Lake Levee and

Drainage Districts, Scott, Morgan, and Cass Counties, Illinois.

Contract No. DACW43-82-D-0083

by7Edwin R. Hajic and David S. Leigh 4.,--Harold Hassen, Principal InvestigatorCenter for American Archeology L

By

US Army Corpsof EngineersSt. Louis District September 1984

IIIABSTRACT

The Meredosia Village and Meredosia Lake Levee and Drainage Districtstudy is the fifth of an ongoing series of combined geologic, geomorphic,and archeological surveys of lower Illinois River valley levee and drain-age districts. Subsurface investigations in Illinois Valley deposits areused in concert with geomorphic analysis and radiocarbon dates toidentify, spatially delimit and date lithostratigraphic units, interpretdepositional environments, and reconstruct the terminal Wisconsinan andHolocene valley evolution. Within this contextual framework, evaluationsof the location and preservation potentials for surface and buried

archeological sites are made.

Ii

ACKNOWLEDGEMENTS

Those deserving special thanks are the many landowners and tenants inthe Meredosia Village and Meredosia Lake Levee and Drainage Districts whoallowed soil coring on their land:

Albert Alhorn G. 0. Head Farms Inc.Henry Alhorn Herbert HinnersJ. J. Alhorn Ruel Hobrock

Bob Banghart Velma D. KineyGary Banghart William KleinschmidtByron Beauchamp Harold C. KuhlmanMrs. Virgil Beauchamp Earl LovekampTom Brackett Edwin LovekampMartin Burrus Leona LovekampDrew Carls Albert MaySteven Carls James McCormickMarion C. Chute James MerrimanEverett Dunham Harold OakesLorance Fricke William PineBob Gregory Zelmer RohlfingEdward Hammon Edgar SouleGary Hammon Freida WeberLarry Hardwick Leland WeberMaurice Hardwick Clarence WinklemanNadine Hardwick Eldon WinklemanRoscoe Hardwick Marlin WinklemanAndrew Harris Michael WinklemanJames 0. Harris Harlan YeckHelen 0. Head

The cooperation of the U.S. Army Corps of Engineers, St. LouisDistrict, in particular Terry Norris, is greatly appreciated.

Alan Goodfield, Illinois Department of Transportation, providedadditional subsurface data.

Field assistance was provided by Julia Clifton and Cynthia Danley.Carbonate and mechanical analyses were performed by Cynthia Danley.Figures were skillfully drafted by Cynthia Danley and Frieda Odell-Vereecken. The final manuscript was processed by Beverly Sexauer andMarjorie Schroeder.

This study was conducted under contract between the Contract Arche-ology Program, Center for American Archeology, and the U.S. Army Corps ofEngineers, St. Louis District, Contract #DACW43-82-D-O083.

The U.S. Army Corps of Engineers Illinois Valley geomorphic andarcheologic surveys are coordinated by Dr. Harold Hassen, Center forAmerican Archeology.

ii

TABLE OF CONTENTS

page

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

Acknowledgements.................. . . ... . .. .. .. .. .. . ...

List of Figures .. ......... ......... ....... iv

Listof Tables. .. ........... ......... ..... vi

Introduction - Problem Statement. .. .... ....... ...... 1

Theoretical Orientation. ..... ......... .......... 2

Research Goals and Methodology. .. .... ....... ........ 4

Location .. ....... .............. ......... 5

Field and Laboratory Methods .. .. ....... ............ 7

Meredosia Village and Meredosia Lake District Geomorphology and SoilGeomorphic Relationships. .. ..... ......... ....... 15

Stratigraphy. .. ............. ......... .... 19

Meredosia Village and Meredosia Lake District Archeology .. .. ... 32

Geomorphic, Stratagraphic, and Archeological ContextualRelationships. .. ... ......... .............. 324

Conclusions ... ............. ......... .... 38

References Cited. .. ........ ......... ........ 42

Appendix A: Core Descriptions. .. ...... ....... ..... 48

Appendix B: Particle Size and Carbonate Data .. ........... 130

Appendix C: Outline of Late Wisconsinan and Holocene Geology ofthe lower Illinois River Valley, by Edwin R. Hajic . . . 133

Appendix D: Scope of Work .. .... ........ ......... 153

LIST OF FIGURES

page

Figure 1. Location of the Meredosia Village and Meredosia LakeLevee and Drainage Districts, Scott, Morgan and CassCounties, Illinois ...... ...................... 6

Figure 2. Location of core holes and cross sections, MeredosiaVillage District ....... ...................... 8

Figure 3. Location of core holes and cross sections, MeredosiaLake District .......... ..................... 9

Figure 4. Geomorphology of the Meredosia Village District . . .. 16

Figure 5. Geomorphology of the Meredosia Lake District .. ..... 17

Figure 6. General soil groupings by texture within theMeredosia Village District ..... .............. ... 20

Figure 7. General soil groupings by texture within theMeredosia Lake District ...... ................ ... 21

Figure 8. Meredosia Village cross-section A-A' .. ......... ... 23

Figure 9. Meredosia Village cross-section B-B'. .. ......... ... 23

Figure 10. Meredosia Village cross-section C-C'. .. ......... .... 24

Figure 11. Meredcaia Village cross-section D-D'. .......... . 24

Figure 12. Meredosia Village cross-section E-E'. .. ......... ... 25

Figure 13. Meredosia Lake tross-section F-F'. ............... ... 26

Figure 14. Meredosia Lake cross-section G-G'. ... ........... ... 26

Figure 15. Meredosia Lake cross-section H-H'. ... ........... ... 27

Figure 16. Stratigraphy, particle size and carbonate data forcore MLC-19 .......... . ..................... 29

Figure 17. Stratigraphy, particle size and carbonate data forcore DLC-28 ........ ...................... ... 30

Figure 18. Location and preservation potentials for surface andburied archeological sites in the Meredosia Villageand Meredosia Lake Districts .... ............. ... 35

iv

LIST OF FIGURES continuedI page

Figure 19. Estimated buried site potentials in the MeredosiaVillage District ......... ................... 40

Figure 20. Estimated buried site potentials in the MeredosiaLake District ............................... 41

Figure C-i. General geomorphology of the lower Illinois RiverI valley, north section, east of the Illinois River . . . 137

Figure C-2. General geomorphology of the lower Illinois Riveri valley, south section ......................... 138

Figure C-3. Longitudinal profile of major geomorphic surfaces,lower Illinois River valley .... .............. ... 139

I Figure C-4. Generalized summary of lower Illinois River valleystratigraphy, depositional environments, and episodes

i of lower Illinois valley history ..... ............ 142

Figure C-5. Schematic cross-section of Illinois Valley .......... 143

IIIIIIIIII

LIST OF TABLES

page

Table 1. Core location, landscape position, and associated SCSsoil, Meredosia Village and Meredosia Lake Districts . . 11

Table 2. Soils groups, by texture . . . ............... 22

Table 3. Known Meredosia Village and Meredosia Lake Districtarcheological sites, cultural affiliation and landscapeposition ........... ........................ 33

Table B-i. Particle size and carbonate data ... ............ .. 131

Table C-i. Lower Illinois River Valley Levee and Drainage Districtradiocarbon dates .... ..................... 135

vi

INTRODUCTION - PRODLDI STATEMT

I Since the late 1920's the Illinois River valley has undergone con-

siderable artificial modification, conducted largely by federal agencies.

An extensive levee system has been constructed along the Illinois and its

major tributaries for flood control and navigation purposes. Floodplain

drainage ditch networks also serve needs of the local farming community.

The U.S. Army Corps of Engineers, St. Louis District, is planning a

program of renewed levee modification and extension of drainage ditch

networks in the lower valley of the Illinois River from Otter Creek

(River mile 15) to Beardstown (River mile 90).

Archeological sites in alluvial contexts are frequently buried by

I sediments indicative of a variety of depositional environments charac-

teristic of dynamic fluvial systems (i.e. Hoyer, 1980; Bettis and

Thompson, 1981; Gladfelter, 1981; Ahler, 1976; Stafford, 1981; Chapman,

1978; Hoffman, 1980). The Illinois River valley is no exception to these

conditions (Wiant, 1980; Hajic and Styles, 1982; Hajic, 1981a; Kraus,

1980; Houart, 1971; Farnsworth, 1976). Levee and drainage ditch con-

struction on and within the Illinois floodplain necessarily requires

excavation and sediment movement, potentially at the expense of buried

archeological deposits. Aware of these archeological concerns, the Corps

of Engineers desires to select borrow locations which would minimize

archeological damage, and still provide construction material with suit-

able engineering properties. The Corps of Engineers has contracted the

Center for American Archeology, Contract Archeology Program, to develop a

predictive model that can effectively estimate the relative potential of

encountering buried surfaces which might contain archeological material

in selected levee and draiage districts (i.e. Scope of Work, Appendix

D). The problem involves identification of possible buried site

locations and their preservation potentials.

I Historically, the Corps of Engineers has partitioned the Illinois

floodplain into a continuous series of levee and drainage districts.

These districts comprise the basic study units of the ongoing project.

Districts extend roughly 7 to 14 km along the valley and are separated by

1I

canalized and/or leveed major valley tributaries. It is within this

organizational framework of selected districts that the predictive

modeling necessarily proceeds.

THEORETICAL ORIENTATION

The Illinois valley has been a changing landscape for at least the

last 13,000 years (Hajic, 1983b; Hajic and Styles, 1982; Butzer, 1977).

Because archeological sites are deposits on landscapes, the quality of

archeological site location predictive modeling capabilities directly

depends upon the degree to which the present landscape, former landscapes

An systematic formational processes are understood. In the strati-

graphic record landscape change by geomorphic processes operating through

time is evidenced. Furthermore, the stratigraphic record holds clues to

archeological site location through interpretation of depositional envi-

ronments by identifying and dating sedimentary units and lithofacies

associations. Consequently, the Corps of Engineers project has been

viewed from inception as a geologic problem as much as an archeological

one. Buried archeological site potentials are most adequately evaluated

in the context of a model of terminal Wisconsinan and Holocene evolution

of the lower Illinois River fluvial system developed from a temporally

grounded stratigraphic and sedimentologic framework. The reconstruction

emphasizes identification of sedimentary units and paleogeomorphic sur-

faces as well as providing interpretations of the depositional environ-

ments and processes responsible for the observed stratigraphy. Further-

more, while broad in scope, the geologic reconstruction emphasizes con-

struction of an absolute time framework which is sufficiently detailed to

be archeologically relevant (see Appendix C, this volume).

Prior to fieldwork, several expectations regarding investigations of

the lower Illinois River valley were outlined: 1) Due to the regional

physiographic position of the Illinois River in the midcontinent, the

geologic history would be potentially complex. The Illinois is tributary

to the Mississippi River and the lower Illinois valley would have adjus-

ted in response to fluvial events in the Mississippi valley (Clayton,

1982; Clayton and Moran, 1982). Simultaneously the Illinois valley has

periodically served as drainageway for variable discharge from the Lake

2

II

Michigan Basin (Hansel et al., in preparation; Evenson et al., 1976;Willman, 1971; Hough, 1958). 2) Fluvial processes are likely to vary

along the 120 km study reach of the Illinois valley at any particular

time. This expectation is largely a consequence of current theoretical

views of fluvial systems and processes. Changes external to a fluvial

system, as well as changes inherent in the system, (i.e. eclipsing a

geomorphic threshold) can trigger a set of complex responses involving

erosion and deposition which may co-occur along different reaches of the

system (Schumm, 1973; 1976).

WithLi a complex natural fluvial system, one event can trigger a

complex reaction (morphologic and/or stratigraphic) as the

components of the system respond progressively to change. This

principal provides an explanation of the complexities of the

alluvial chronologies, and it suggests that an infrequent event,

although performing little of the total work within a drainage

system, may, in fact be the catalyst that causes the crossing of

a geomorphic threshold and the triggering of a complex sequence

of events that will produce significant landscape modification

(Schumm, 1973:307).

3) In addition to evaluating buried site potential, the collection of

* cores for a three dimensional reconstruction would provide a wealth of

paleoenvironmental data. 4) Due to the mandated organizational framework

of the valley, subsurface investigations would be intensive within indi-

vidual districts selected by the Corps of Engineers and proceed one

district at a time. The model would ultimately be for the entire lower

120 km of the Illinois valley although not all districts would be ex-

amined. The predictive capability of successive district studies would

increase as the geologic model progressively developed. 5) A large

number of radiocarbon dates would be required to develop the geologic

*model at an appropriate scale.

3

RESEARCH GOALS AND METHODOLOGY

The primary research goal, as outlined in Corps of Engineers scope

of work, is to model location and preservation potentials for buried

archeological sites in Illinois River valley levee and drainage dis-

tricts. While the goal is archeological in nature, achieving it requires

utilizing not just geomorphic and geologic techniques and methods, but

more importantly, the interpretations of landscape change and development

resulting from these techniques and methods.

Unlike previous geological and geomorphological investigations in

the lower Illinois River valley (Butzer, 1977; Rubey, 1952; Root, 1935),

most effort is being invested in subsurface stratigraphic investigation

using solid cores collected with a Giddings hydraulic soil probe.

Holocene sediments may be in excess of 15.2 m (50 ft.) in thickness and

valley-bottom outcrops are normally limited to a ftvi meters exposed in

drainage ditches. The cores are being used to identify and trace deposi-

tional units, buried surfaces and soils; identify vertical ana lateral

stratigraphic relationships; interpret depositional environments; define

paleochannel locations and morphology; recover datable organic material;

and on occasion recover evidence of cultural occupation. Transverse

valley cross-sections are constructed to provide a three-dimensional

stratigraphic framework. Known surface site distributions from a variety

of largely systematic surveys are being examined for each district and a

limited survey at core locations is conducted. Under separate scopes of

work, surface surveys are being performed along corridors paralleling

levees (c.f. Hassen and Batura, 1983). These surveys normally lag behind

the geologic/geomorphic investigations. Supplementing the principal

research goals, the solid cores contain a wealth of paleoenvironmental

data. Organic matter, molluscs and gastropods are at times abundant.

The scope of work does not allow faunal and floral analyses; however, the

collections have been curated for future study. Also, information pro-

vided from cores allows the alluvial record of the lower Illinois valley

to be integrated into the regional late Wisconsinan and Holocene se-

quence. As the Illinois system is intimately linked through fluvial

processes and responses to both the Mississippi valley and the Lake

Michigan Basin, its evolution may provide clues to the timing of events

in these related systems.

The intent of this report, the fifth in the series of studies of

Illinois River levee and drainage districts, is to evaluate the potential

of encountering buried archeological sites in the Meredosia Village and

Meredosia Lake Levee and Drainage Districts. The first report of this

series (Eldred and Spankey Districts; Hajic and Hassen, 1980) (Figure 1)

focused on the recognition and familiarization of soils, sediments,

valley geomorphic features and their interrelationships. Rough approxima-

tions of buried site potentials were made. In addition to identifying

this potential in the Nutwood District (Hajic, 1981b), it was noted that

shallow subsurface sediments could be divided into seven distinct units

traceable within the district. It was further noted that the distribu-

tion of some of these units had little or no relationship to the present

floodplain morphology.

In the Hartwell and Hillview Districts (Hajic, 1981c; 1983b) empha-

sis was placed on identifying the continuity and variability of the seven

sedimentary units defined in the Nutwood District. The definition of

l unit boundaries was refined. A limited number of radiocarbon dates from

the Nutwood, Hartwell and Hillview Districts (see Appendix C, Hajic,

1983b) allowed construction of an initial temporal framework for the

sedimentary units. At this stage, radiocarbon dates are second only to

stratigraphic data in their importance to the project, and a considerably

larger number of samples must be run for the model to be truly effective.

I The Meredosia Districts provide an opportunity to investigate relict

landforms and associated sediments which are absent from previously

I studied Illinois Valley districts located farther to the south (Figure

1).

I LOCATION

The Meredosia Village and Meredosia Lake Levee and Drainage

Districts are located in northwestern Scott, western Morgan, and south-

western Cass counties (Figure 1). The Meredosia Village District is

II

LEVEE DISTRICTS -

I z NUTWOOD

2=ELDRED- '

4 4: H)LLV)EWCHAG '-5 =MEREDOSIA S

6 6z MEREDOSIALAKE---------- KOI1-O#

JII

I - 3

M~isso~jr ST LOUIS

I 0 MILES 40

0 KMI 50

Figure 1. Location of the Meredosia Village and Meredosia LakeLevee and Drainage Districts, Scott, Morgan and CassCounties, Illinois.I 6

I

bounded by canalized Coon Run to the south and southeast, and by levees

on Willow Creek to the north. To the west are Illinois River backwaters,

most notably Smith Lake and the southern extent of Meredosia Lake, and

the Illinois River by the town of Meredosia (Figure 2). Valley margin

bluffs form the eastern boundary of the northern half of the district and

are 200-300 km east of Coon Run in the southern half. The Meredosia

Village Levee and Drainage District spans Illinois River miles 67.0 to

72.9.

Southern and northern boundaries on the Meredosia Lake Levee and

Drainage District are levees of Willow Creek and Indian Creek respective-

ly (Figure 3). To the west is Meredosia Lake. The eastern boundary is

primarily state Highway 100. The Meredosia Lake Levee and Drainage

District is between Illinois River miles 72.9 and 79.0.

At Willow Creek, the Illinois Valley is 13 km wide. To the south it

gradually tapers to 5 km at its mouth. Immediately north of Willow

Creek, it abruptly widens to over 16 km. The Illinois River hugs the

western valley margin for its first 6? river miles, but uncharacteristi-

cally diverts up to 7.5 km away from the western bluffline at the lati-

tude of the Meredosia Districts.

FIELD AND LABORATORr METHODSTo reconstruct the three dimensional Holocene valley structure in

the Meredosia Village and Meredosia Lake Levee and Drainage Districts,

coring was a necessity. One hundred twenty-seven solid cores 6.4 cm (2.5

in) or 8.9 cm (3.5 in) in diameter were extracted with a trailer mounted

Giddings hydraulic soil probe. Additional sampling, depending upon sedi-

ment type, was accomplished with a 5.1 cm (2 in) flight auger.

The Giddings machine retrieves a largely undisturbed solid core by

hydraulically pushing a hollow 1.25 meter (4 ft) core barrel into the

ground. When the tube is retracted, the sediment/soil core is gently

retained within the tube by friction at the cutting bit until shaken out

the top of the core barrel by the operator. A continuous core is ob-

tained by returning repeatedly to the same hole. The machine cannot

7

-'-PE

-ITI

Figure 2. Location of core holes and cross sections, MeredosiaVillage District.

8

A ORPS DF FN3tNEERS

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Fiur 3. Loaino oehlsad rs etos eeo

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penetrate gravels and some sands, nor can it retrieve saturated sediments

not sufficiently cohesive to hold an open hole while the tube is retrac-

ted and being emptied. The latter condition was not a problem and most

cores were terminated due to refusal on pebbly sand or sand.

After coring, a limited surface survey for archeological material

was conducted within approximately 6 m (20 ft) of the core hole. The

purpose of the surface survey was to determine presence or absence of

archeological sites. The surface survey was not intended to determine

specific parameters of any site discovered, and only diagnostic or unique

material was to be collected.

Evaluation of potential sediment/soil core hole locations necessi-

tated consideration of the following aims: 1) construction of valley

cross-sections; 2) identification of subsurface sediments and sedimentary

relationships; 3) tracing of terraces and deposits of known age and

origin; and 4) sampling of a variety of soil types and floodplain geomor-

phic features. Fifty percent of the cores in the Meredosia Levee and

Drainage Districts were required to be taken within a corridor paral-

leling the main and lateral levees (see Scope of Work, Appendix D). Crop

cover and problems with obtaining access necessarily restricted coring in

some preferred locations. Core locations were selected with the aid of

black and white, and color aerial photographs, topographic maps, soil

series maps and information obtained from preceeding cores. Core hole

and cross-section locations are indicated on Figures 2 and 3 and listed

with reference to the cadastral system in Table 1. Each core was ex-

amined in the field, briefly described, and wrapped in plastic wrap and

aluminum foil for transport. More detailed descriptions were performed

under uniform conditions in the field laboratory using standard USDA soil

terminology (Soil Survey Staff, 1975). Because of time limit/ions, only

depth, interval, color (moist Munsell), texture, structure and boundary

were described. Although developed primarily for till and loess de-

posits, standard weathering zone terminology (Hallberg, Fenton and

Miller, 1978) was useful in describing carbonates and oxidation state

(see Appendix A for an explanation of the terms "oxidized", "deoxidized",

and "unoxidized"). Engineering textural descriptions (U.S. Army Engineer

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Waterways Experiment Station, 1960) for major units were also recorded

per request in the Scope of Work (Appendix D). Any special features or

inclusions (organic matter, charcoal, gastropod and bivalve shells,

krotovina, lithic debris) were noted. Various units were sampled, air

dried and stored f'or future analyses of particle size, clay and sand

mineralogy, carbonates, C-14 and identification of micro- and macro-

botanical organic matter. Core descriptions are presented in Appendix A.

Additional subsurface data were obtained from the Corps of Engineers, St.

Louis District, Illinois Department of Transportation, and Illinois River

maps (Woermann, 1904).

Although stratigraphic data derived from cores provides the primary

data base, laboratory analyses were deemed necessary to begin to charac-

terize lithostratigraphic units and verify field descriptions. Methods

and procedures of chemical and physical analyses employed are considered

standard for the evaluation of unconsolidated Quaternary sediments and

soils in the midwest (Hallberg, 1978; 1980). Particle size analyses were

completed using the method of Kilmer and Alexander (1949) as modified by

Walter et al. (1978). Calcite and dolomite were determined gasometrical-

ly using the Chittick apparatus (Dreimanis, 1962). Values were

calculated using the following empirical equations for the graphed

lines of Dreimanis, as reported by Walter and Hallberg (1980):

% calcite F (0.232)

% dolomite E (0.223) + 0.3.

The values E and F are corrected volumetric readings of CO2 for dolomite

and calcite respectively. Chemical and physical data are tabulated in

Appendix B.

Cross-sections and geomorphologic maps (see below) were constructed

and interpreted by utilizing both new core hole descriptions and other

previous boring records, black and white, and color aerial photographs,

color infrared aerial imagery, topographic maps and soils data. Land-

owner interviews also provided valuable information on subsurface sedi-

ments as most farmers have excavated deep wells or have sunk sand points

14

on their property.

Because of the complex nature of fluvial sediments and the sampling

intervals, cross-sections are generalized to some extent. Nevertheless,

a clear stratigraphic picture emerges. All elevations are based on

Illinois River floodplain topographic maps with 2 ft contour intervals

(U.S. War Department, 1944) with vertical datum plane referred to 1929

General Adjustment USC & GS (Mean Sea Level). Spoil from drainage ditch

construction since 1944 has been included in core descriptions, but was

omitted and adjusted for in cross-sections.

IER DOSIA VILLAGE AND NEREDOSIA LAKE GEONORPDOLOGY

The Meredosia Districts differ from previously studied districts

(Figure 1) because they encompass several geomorphic surfaces and fea-

tures which are not represented in the southern half of the lower

Illinois valley. Two previously defined terraces, the Bath Terrace (Wan-

less, 1957; Styles, 1984; Hajic, 1983b) and Bluffs Terrace (Hajic, 1983b;

Styles, 1984) in part border unburied remnants of the Bug Island Paleo-

channel, a broad, straight Illinois River paleochannel (Figures 4 and 5).

Also represented are extensive alluvial fans and a broad range of allu-

vial features associated with tributary creeks which have traversed much

of the Bug Island Paleochannel after abandonment by the Illinois River.

The Bath Terrace has almost a continuous cover of eolian dunes at-

taining elevations over 143 m (470 ft), but more commonly ranging between

139 m (455 ft) and 142 m (465 ft). Where dunes are absent, the sandy

surface is at about 137 m (450 ft). One large Bath remnant extends the

full length of the western side of the Meredosia Village District while

two large remnants are preserved in the Meredosia Lake District.

Less obvious is the Bluffs Terrace which also has a primarily sandy

surface, but may on occasion have a silt loam surface. It is found at

elevations ranging from 133.5 m (438 ft) to 134.7 m (442 ft). The Bluffs

Terrace sometimes has low eolian dunes or reworked dunes that may reach

elevations of about 137.8 m (452 ft). Remnants are preserved adjacent

to the east side of Bath Terrace remnants in both districts and as

15

J'6

ADA

Figure 4. Geomorphology of' the Meredosia Village District.

16

IIE I

4Q

Fiue5Iemrhlg fteMrdsaLk itit-- ~->17

isolated remnants in the Bug Island Paleochannel. The latter are relict

channel bars or islands and generally have low eolian dunes associated

with them. The boundary between the Bath and Bluffs terrace is at times

indistinct, but generally mapped where large dunes occur on the Bath

Terrace. North of the Meredosia Lake District and just south of

Beardstown the Bluffs Terrace slopes up to and apparently merges with the

Bath Terrace. The close association at the Bluffs terrace with the Bug

Island Paleochannel suggests the Bluffs may be a related floodplain

surface.

The Bug Island Paleochannel derives its name from one of the mid-

channel bars/islands (now considered Bluffs Terrace remnants) that is

approximately 4 km south of the triple junction of canalized Coon, Eagle

and Wolf Run (Styles, 1984). One reach of the paleochannel is located in

the two districts and extends their lengths (Figures 4 and 5). In the

Meredosia Village District, the paleochannel is located between the

eastern bluffline and Bath and Bluffs remnants. Terrace remnants bound

either side of the paleochannel in the Meredosia Lake District (Figure

5). On high altitude aerial photographs, the paleochannel appears at

least 8 to 10 times the width of the present Illinois River channel.

In the Meredosia Village District, most of the Bug Island Paleochan-

nel has been filled by a broad apron of coalescing yet distinct alluvial

fans. Major fans occur at the mouths of Wolf Run, Eagle Run, Spring Run,

and Coon Run. The westward extent of Eagle Run fan has been restricted

by a Bluffs terrace remnant. Tributary creek channel traces on the

fans exhibit both braided and meandering patterns. At times, the larger

creeks extended beyond their fans and eventually terminated in small

splays and distributary networks probably in shallow lakes, in the Bug

Island Paleochannel.

In the Meredosia Lake Levee and Drainage District, much of the

paleochannel has been modified by fluctuating coarses of Willow Creek and

Indian Creek. Indian Creek is now diverted and forms the northern dis-

trict boundary. In past times it flowed south on the east side of a

large Bath Terrace remnant, then west and to the north of a large channel

18

I

bar/island (Figure 5). Meandering channel traces of Indian Creek are

clear in high altitude aerial photographs and may have reworked some

Bluffs terrace remnant margins east of Highway 100 (Figure 5). Willow

Creek has been similarly active, reworking much of the Bug Island Paleo-

channel between canalized Willow Creek and the Cass-Morgan county line.

The resulting landscape in this area is a low hummocky topography of

infilled channels, low natural levees and bars.

Along the eastern margin of Meredosia Lake is either a natural levee

remnant deposited by a former Illinois River or an eroded Bluffs terrace

remanant (Figure 5).

Major soils (those formed over largest areas) (Figures 6 and 7;

Table 2) on the Bath Terrace are the Plainfield sand and Sparta loamy

sand. These reflect the largely dune mantled terrace surface. While

sharing some soil similarities, the Bluffs Terrace also has Keomah silt

loam, Hoopeston sandy loam, Orio silt loam, and even some Ambraw clay

loam in depressional areas. Major soils in the Bug Island channel, where

not buried by upland derived sediments, include Darwin silty clay,

Beaucoup silty clay loam and Ambraw clay loam. Worthen and Littleton

(Table 2) silt loams dominate the proximal and medial alluvial fans and

reflect the upland origin of the sediment. Dupo silt loam is mapped on

distal fans where upland derived sediments are thin and underlying Bug

Island Paleochannel sediments may be incorporated in the lower soil pro-

file. Grouping the soils by texture (Table 2) illustrates a close corres-

pondence to the geomorphology of the districts (Figures 6 and 7).

STRATIGRAPHI

Eight lithostratigraphic units were defined on physical criteria

observed in cores. Eight valley cross-sections illustrate stratigraphic

relationships of these units and shallow subsurface valley structure in

the Meredosia Village and Meredosia Lake Levee and Drainage Districts

(Figures 8-15).

SUi _L This unit consists of oxidized and leached loamy fine sand

to pebbly medium and coarse sand with depth. In the surface soil, tex-

19

I C.101

I -~ C

-E-00 1

IE ft.

-0-IS0I

Fiue6Ieea ol gopig ytxuewti hIeeoi ilg itit

I2

DD

A C

~D

Figure 7. General soil groupings by texture within theMeredosia Lake District.

21

Table 2. Soils Groups by Texture.

Texture Soil Series

clay, clay loam, silty clay loam, Houghtonsilty clay, muck Palms

AmbrawBeaucoupSawmillTiceDarwin

silt loam ArenzvilleDupoKeomahLittletonOrioRaddleTallulaThorpWagnerWorthen

loam LaflogueMedwayRoss

sand, loamy sand, sandy loam WatsekaSpartaHoopestonOnargaGilfordPlainfieldBloomfieldMorocco

22

0

48

_145/

I 470

I 460 -_40

I 450-

4

I440- -15

430-I '30 20 FEET 30420- 0 MjETERS 000

IOL SAND (HENRY FORMATION)I2 DU SAND (HENRY FORMATION (?)) 5 C/O, L/U SILT LOAM ond SILT ICAHOKIA3 DU, LAMINATED and BEDDED SILT, ALLUVIUM - ALLUVIAL FANS)

41 5 CLAY 0 nd SAND (EQUALITY FORMATION?) 8 OIL, L/U SILTY CLAY, SILTY CLAY LOAM and PEAT

TI0'2 4 OL FINE SAND (PARKLAND SAND) (CAHOKIA ALLUVIUM - BUCK LAKE MEMBER)

zFigure 8. Meredosia Village cross-section A-A'.

46 __ 40'8

I 135

430

-130OL SAND (HENRY FORMATION)

2 DU SAND (HENRY rORMA~hON(7l)

420- 3 OU, LAMINATED and BEDDED SILT, CLAY

and SAND (EQUALITY FORMATION?) 8 0,L, L/U SILTY CLAY, SILTY CLAY LOAM and PEAT5 O/D, L/U SILT LOAM and SILT ICAHOKIA CAHOKIA ALLUVIUM - BUCK LAKE MEMBER)

ALLUVIUM - ALLUVIAL FANS) P__ LE_ 30006 OL SILTY CLAY LOAM and SILT LOAM (CAHrKIA .E 00

ALLUWVIUM -OTHER UPLAND DERIVED ALLU', UM)!9&i410 '125 0 mETERS '000

IFigure 9. Meredosia Village cross-section B-B'.23

II

> 0470

C

460I '40

450 ,

35

440-

I3430-

I 00 EET 3000

. 0 METES 000420 OL SAND 'HENRY PORMAT,0N) 5 /0 -j I -7 CM 4n' S AHOKIA ALL.JVjM -

2 DU SAND 'HENRY P0RMAT'ON0)j) A-.. VA4L. PANS)

3 DU, LAMINATED Old BEDDED SILT, _aY B OIL. -U SILT

Y CLAY SILT Y

CLAY LCAM Old "EATold SAND (EQUALITy PORMAT ON7) 0 ALLJVIUM " BUCK LAKE MEMBER

4,0 '125

0 Figure 10. Meredosia Village cross-section C-C'.0

I t I r i iID D'

460

35

440

430.30

420 -'IET 3000

IETES 000

3L SAND 'HENRY 'OQMATiON) -CAM d 3,9 CAY0I ai_- UM-4?) 25 1 DU SAND (,EPY RCQMA ION ALI-,jA .AL ANSI, OAM NA oEC 9 )®m0 E E Y _r, ' .Y _A.-Y.

Y ' Y -_ 02 O d EA -

I'~d SAND EGUA.. ' r A'm AUI A-E MEM9E6

Figure 11. Meredosia Village cross-section D-D'.

24

Iw

I LU

I 019~~ --f

o

ujW

0-1w 4

- -j

0I0 L)

-I 02

0

020

~J0- 0

LUi

Sn 0 J)

ii 0 0 _0 0, CL

vn cN-I >0(I . LI 25 -

0

L- 0- ~

uJi w ~J _j J j _j j .J j _ja. 0 00 0 00 0 0 0

460-.40 I I II

450-

440135 4

430 1303

420-

2o FEET 3000

0 METERS 000

41 f15 ILSNDCLAYLFOMTIN 4 OLFINE SAND (PARKLAND SAND)ALVIM

DU SND HENY FRMATON()) OLSILTY CLAY LOAM and SILT LOAM (CAHOKIA

Figure 13. Meredosia Lake cross-section F-F'.

z0

> 0O, M~~ Nn cm f a)C

0 OOO 0 000

000o000 0 0 30

460--140

450-

354

440-

430430- 0 PEET 3000

0 METERS .000

420-

2L 2 DU SAND HENRY PORMATiON),))

3 '3U, -AMI NATED and BEDDED SILT, CLAY

am d SAND EQUALITY POPN4AT ON)

_L 4 OL PINE SAND PaRK~LAND SAND)410- -25

Figure 1J4. Meredosia Lake cross-section G-Gf.

26

O

V> L Q

._j

460 -- 140 I I

450

430-6

~13

420 -

~41

0 0EET 3000

0 METERS 1000

400 -120

2 DU SAND (HENRY FORMATION 7)) 6 OL SILTY CLAY LOAM and SILT LOAM (CAHO KIA

3 DU, LAMINATED ond BEDDED SILT, ALLUVIUM - OTHER UPLAND DERIVED ALLUVIUM)

CLAY and' SAND (EQUALITY FOR- 7 U, L/U SI LTY CLAY and CL AYE Y S? LT (GAHOKI AM AT ION 7) ALLUVIUM - HARTWELL MEMBER)

4 OL FINE SAND: (PARKLAND SAND) 8 O/U, L/U SILTY CLAY, SILTY CLAY LOAM ond PEAT

(CAHOKIA ALLUVIUM -SBUCK LAKE MEMBER)

Figure 15. Meredosia Lake cross-section H-H'.

27

tures may be fine sandy loam and there is weak indication of original

stratification. The unit occurs beneath dunes on the Bath Terrace

(Figures 8-13). The Bluffs Terrace, when adjacent to the Bath, is also

developed on Unit 1. Corps of Engineers boring records indicate this

unit to be in excess of 9 m (30 ft) thick. The unit belongs to the Henry

Formation (Willman and Frye, 1970) which consists of outwash sand and

gravel of Wisconsinan age.

U= 2,. Most cores terminated in this unit and it occurs throughout

the Bug Island Paleochannel as a basal unit. Unit 2 consists of deoxi-

dized to unoxidized, unleached fine to medium sand (Figures 8-15).

Coarse sand with very fine to fine pebbles occur at depth. The upper

meter is most commonly interstratified with laminae and thin beds of

deoxidized, unleached, sandy silt to silty clay. The silty laminae are

occasionally organic, and may consist entirely of fine pieces of uncar-

bonized organic matter. The Henry Formation is the closest formaly de-

fined correlate.

_U= a is also confined to the Bug Island Paleochannel and overlies

Unit 2. The contact is abrupt, but in most cases conformable with Unit

2. Unit 3 consists of interlaminated and interbedded sediments of a wide

textural range. The core of the unit is commonly a strongly laminated to

thinly bedded silt (Figures 16 and 17). It is generally deoxidized and

unleached, but often contains some reddish brown silt strata or clay

laminae that are leached or only very slightly effervescent with dilute

hydrochloric acid. Commonly underlying the unit is a thin bed of oxi-

dized, unleached or leached fine or medium sand. Fine sand may be inter-

stratified throughout the unit. Overlying the unit core are generally

sandy clay loam, loam, or clay loam strata, or strongly laminated silt to

silty clay loam. Laminae of fine pieces of uncarbonized organic matter

are common both above and below reddish brown strata. Unit 3 was de-

posited primarily in slackwater or lacustrine environments in the Bug

Island Paleochannel with occasional fluvial input. The closest litbo-

stratigraphic correlate formaly defined is the Equality Formation

(Willman and Frye, 1970).

28

I MILC -19

STRATIGRAPHY DEPTH PARTICLE SIZE CARBONATES

u 00 0 20

w N 00 0J 0L

Ap LL U44L 'AllA P l) MN T UNI T 5

Al - CALCITE82t DOLOMITE

5

Alb,

-~-2ID 9 ,. .....

I 0J CL,.. . . .. . .. . .LL . ... ... ... ...

0 ......U........I. ...< SILT.......

... .. .....0.. .. .. ... .. ..I PvAL...........20.

.. . . . . .I3 . . . . . . . . . . . . . . . . . . ..____ ___ ___

Figure16. Sratigaphypartile.sie.a.dcarboate.dta..oI..core........D UI-. ............ .. .. . .. . .. .

DLC-28

STRATIGRAPHY DEPTH PARTICLE SIZE CARBONATESo (%M) N%

< U U0 3uLO 0 U- .0 50 100 0 5 '

0 __C I

LAJ EOLIf.N SAND (UNIT 4)Z Alb,

................o.. CALCITE......... 0: DOLOMITE

C Cr

82! L ACUST RINE i: ::-

22 S ED. ME NT ?)5 .::*:~§..

K22(U I )0a . . . ...

C.. ... ..I- .-- ...

.. .. .. ...... ....

823b2-. .. .. .. .

- 2. . .. . ..

LUb

. . . . .. .. ..

Z Z

UJzb .. . . ..

OL J~d..........SAN

10 Cu.. . .. .

zL LAU -IN

SEOIME20Z

(U IT3:D IL

7. . . .. . .

O/DL . ..... .....

S. _____._____

Figur 17. tratgraph, paticlesizeand . rbonte.daa..ocore.........

30. . .. . .

I

i Unit _k is composed of oxidized and leached fine sand of eolianorigin (Figure 17). This unit comprises dunes over Unit 1 and less com-

monly, Unit 3. In only a few instances is there an intervening paleosol,

and when present, it is very weakly developed. Unit 4 belongs to the

Parkland Sand (Willman and Frye, 1970).

Unit a is located along the eastern half of the Meredosia Village

District and consists of upland derived silt loam deposited primarily as

alluvial fans (Figures 8-12). Colluvial deposits are also mapped as Unit

5. The uppeo, fan deposits are weathered and leached, having oxidized to

deoxidized colors. In most fans, one or more tracable buried soils

occur. The lower part of Unit 5 is laminated with the distinctness of

laminae increasing with depth, particularly where fans are thickest.

Well preserved laminae suggest either rapid deposition, or fan delta

deposition in standing water. Carbonates also pick up in lower Unit 5

sediment (Figure 16). Also common to the lower part of the unit are beds

of silty clay loam which are slightly weathered. Basal fan sediments

are conformable with the underlying Unit 3, and sometimes grade down into

very strongly laminated deoxidized, unleached, silt and very fine sand.

Laterally, Unit 5 interfingers with or buries Unit 8. It also is later-

ally continous with or buried by Unit 6, and basal fan sediments may be

laterally continuous with youngest Unit 3 deposits in the western part of

the Bug Island Paleochannel. Unit 5 is currently mapped as part of the

Cahokia Alluvium (Willman and Frye, 1970).

Unl .6 consists of oxidized and leached silt loam and silty clay

loam largely of upland origin. It occurs most commonly in the Bug Island

Paleochannel, especially in the vicinity of abandoned Willow and Indian

Creek channels in the northeast part of the Meredosia Village District

and southeast part of the Meredosia Lake District (i.e. Figure 12). Unit

6 was deposited by tributary creeks primarily as natural levees, splays

and overbank deposits. It overlies Unit 3 and laterally can be

interstratified with Units 5 and 8. Unit 6 is part of the CahokiaI Alluvium.

_U= 7 is located only in cores DLC-43 and DLC-44 (Figure 14), west

I31I

of the western Bath Terrace remnant in the Meredosia Lake District. This

unit consists of unoxidized and leached silty clay and clayey silt of

slackwater origin. It is probably equivalent to the Hartwell member of

the Cahokia Alluvium defined and described in districts to the south

(i.e. Hajic, 1983b). Here it is underlain by Unit 2(?) and uncon-

formably overlain by Unit 6.

_U= -a consists of leached silty clay loam and silty clay which is

commonly organic. It is the surface unit in the Bug Island Paleochannel

where alluvial fan and tributary creek deposition has not occurred

(Figures 8-12, 15). In the southern part of the Meredosia Village dis-

trict peat and peaty silty clay textures dominate. Here the unit con-

tains abundant gastropods and bivalves, and is calcareous. Unit 8 was

deposited in swamps and shallow intermittant lakes in the Bug Island

Paleochannel following channel abandonment. It may be interstratified

with Units 5 and 6. At least part of Unit 8 may be equivalent to the

Buck Lake member of the Cahokia Alluvium defined and described in dis-

tricts to the south (i.e. Hajic, 1983b).

MERMOSIA VILLAGE AND MEREDOSIA LAKE DISTRICT ARCHEOLOGY

One previously unrecorded archeological site was documented during

the course of this study. The Marlin Winkleman site is located immedi-

ately north of core DLC-35 in the northernmost part of the Meredosia Lake

District. It occurs just north of a dune on the Bath Terrace. The site

consists of a light scatter of chert debris, and no retouched lithics

were found.

Eighteen previously recorded sites in Center for American Archeology

files occur within the Meredosia Districts (Table 3). The sites range

in age from Middle Archaic through Mississippian. They are all as-

sociated with the Bluffs Terrace or Bath Terrace or related dunes except

the Sunset Beach site located on a probable relict natural levee of the

Illinois River.

32

Table 3. Known Meredosia Village and Meredosia Lake District ArcheologicalSites, Cultural Affiliation, and Landscape Position.

Cultural Affiliation Landscaoe Position

Willow Creek Late Woodland Bluffs terrace marginRoscoe Archaic, Late Woodland dune on Bath TerraceHoney Point Late Archaic thru dunes on Bluffs terrace

Late WoodlandShearl Middle and Late Archaic dune on Bluffs terrace(?)Sunset Beach Middle Woodland relict natural levee(?) of

Illinois River, now beachof Meredosia Lake

Wells Early(?) and Late Woodland Bluffs Terrace marginChute indeterminate dune on Bath TerraceDawson Middle Woodland thru Bath Terrace

MississippianMeredosia Middle and Late Woodland dunes on Bath TerraceNational Starch Early and Late Woodland eroded Bath Terrace(?)Virginia Holding Late Woodland Bluff TerraceCo.

Ruthless indeterminate Bluffs TerraceMeadowlark indeterminate Bluffs TerracesNorth Star indeterminate Bluffs TerraceSmall Star indeterminate Bluffs TerraceEleana indeterminate Bluffs TerraceHahn Late Woodland Bluffs TerracePessina indeterminate Bluffs Terrace

Cultural chronology of the lower Illinois River Valley drainage:

Culture Group a (..

Historic post 650Mississippian 850- 650Late Woodland 1500- 850Middle Woodland 2050-1500Early Woodland 2800-2050Late Archaic 4500-2800Middle Archaic 7000-4500Early Archaic 9500-7000Paleo-Indian 11000-9500

33

GEOMORPHIC, STRATIGRAPHIC, AND ARCHECLOGICAL CONTEXTUAL RELATIOMSSIPSi A model for predicting site location potential for both buried and

surface manifestations for specific cultural groups in the Meredosia

Districts is summarized in Figure 18. The evaluation is based upon the:

1) evolving reconstruction of the lower Illinois Valley landscape history

(see Appendix C, this report); 2) three dimensional reconstruction of the

Meredosia Districts based upon core stratigraphic data (i.e. the spatial

location of lithostratigraphic units within the districts): 3) age and

depositional origin of lithostratigraphic units; 4) identification and

location of buried surfaces and soils; 5) present geomorphic configura-

tion of the valley, relationships between known archeological sites,

geomorphic features and geomorphic surface ages, and relationships be-

tween geomorphic surfaces and the age and origin of underlying deposits.

While absolute certainty in predictions is unattainable, it is felt

Figure 18 represents very close approximations, given the extent of

information upon which they are based.

Seven radiocarbon dates from the Bug Island Paleochannel system

indicate it was cut prior to about 14,590±240 B.P. (ISGS-1285) (see

Appendix C, this report) and was intermittantly active until about

9830±160 B.P. (ISGS-1282). Six of the dates were from lacustrine Unit 3

and fluvial Unit 2 at or near the contact with Unit 3. The next to

youngest date is 12,360±240 B.P. (ISGS-1283) from Unit 3 which

corresponds with the end of the Deer Plain lake phase in the lower

Illinois valley (see Appendix C). The youngest age from Unit 2 is

9830±160 B.P. (ISGS-1282), Core MLC-29 (Figure 12), which indicates

intermittent fluvial reactivation of the western side of the Bug Island

Paleochannel system from which the dated material was obtained.

The Bath Terrace probably formed when the Bug Island Paleochannel

system developed (see Appendix C, this report). The Bluffs Terrace,

which consists of several mid-channel bars or islands in the Bug Island

Paleochannel and what appears to be reworked or incised Bath Terrace

margins, formed when the Bug Island channel was active but before about

9800 B.P. (see Appendix C, this report).

34

LOCATION AND PRESERVATION POTENTIALS FORSURFACE AND BURIED ARCHEOLOGICAL SITES:MEREDOSIA VILLAGE AND LAKE DISTRICTS

SURFACE BURIEDGEOMORPHIC SURFACES DEPOSITIONAL UNITS

CULTURAL AGE A" b' ,. ,,GROUP B.P <e ",'" ".",HISTORIC 4- + + + + + - - - : - ]MISSISSIPPIAN + - - I - - -+ - -

LATE WOODLAND 0 + - + + -+ + + -

MIDDLE WOODLAND 2000 -+ +

+ +

+ + +

+

EARLY WOODLAND + + + + + 4- + -

3000 -

LATE ARCHAIC400 4+ +4+ + -4 - - - - 14-i 4+ +- - + -+

4000

5000

MIDDLE ARCHAIC +- 4 + - - --+ + + -I- + 4 - - +6000

7000

EARLY ARCHAIC 4- + + + 4- -+ -- 4- " + - --4-

9000-

PALE"OINOIAN 1,0

,O00{0 - + + +--

12,000

I 13,000

- NO POTENTIAL + MODERATE POTENTIAL

- + LOW POTENTIAL + + HIGH POTENTIAL

DEPOSITIONAL UNITS

I OL SAND (HENRY FORMATION) 6 OL SILTY CLAY LOAM and SILT LOAM (CAHOKIA2 DU SAND (HENRY FORMATION?) ALLUVIUM - OTHER UPLAND DERIVED ALLUVIUM)3 DU, LAMINATED ond BEDDED SILT, CLAY 7 U, L/U SILTY CLAY and CLAYEY SILT (CAHOKIA

and SAND (EQUALITY FORMATION ?) ALLUVIUM - HARTWELL MEMBER)4 OL FINE SAND (PARKLAND SAND) 8 O/U, _/U SILTY CLAY, SILTY CLAY LOAM and PEAT

5 O/D, L/U SILT LOAM and SILT (CAHOKIA (CAHOKIA ALLUVIUM - BUCK LAKE MEMBER)

ALLUVIUM - ALLUVIAL FANS)

I Figure 18. Location and preservation potentials for surface andburied archeological sites in the Meredosia Villagei and Meredosia Lake Districts.

35I

Therefore both the Bath Terrace and Bluffs Terrace surfaces were

available for occupation to all cultural groups. The underlying sedi-

ments of Unit 1 can be practically eliminated from buried site considera-

tion due to antiquity and origin as outwash aggradation. Similarly,

sites will probably not be located within Unit 2. This unit represents

bed load sand when the Bug Island Paleochannel was an active sluiceway.

The interstratified finer units in the top meter probably represent

subsequent lacustrine deposits which accumulated with initial channel

abandonment or initiation of subsequent valley lake phases. In the Bug

Island paleochannel-filling Unit 3 there is only a low potential for

encountering Paleo-Indian camp sites. The strongly laminated to thinly

bedded unit is primarily lacustrine or slackwater in origin with occa-

sional fluvial input of sands. The unit is found over a range of eleva-

tions that parallel the top of Unit 2. Fluctuations of valley lake

levels between circa 12,000 B.P. and 10,000 B.P. (see Appendix C, this

report) would have resulted in large horizontal shifts of lake shorelines

and near shore environments. It is possible that younger Unit 3 surfaces

were at times briefly exposed and available for occupation, and thus the

low potential.

Dunes in the Meredosia Districts are primarily relict features.

Dunes occur on the two sandy terraces and occasionally on Unit 3 silts;

no eolian sand bodies were identified in or on alluvial fans. Several

dunes encroaching upon the Bug Island Paleochannel from the west are

probably due to reactivation as a result of modern farming. Farming may

also account for several blowouts on the Bath Terrace. Unit 4 dune sand

is considered to have a high potential for containing buried cultural

material of all time periods even though the latest dune forming activity

was probably shortly after 10,900 B.P. (Appendix C, this report). Burial

is possible because of local historic reactivation and the action of soil

processes in loose sandy sediment which may vertically move larger ob-

jects down the soil profile. Local farmer Henry Likes indicated to us

that several decades ago, before intensive deep plowing, archeological

sites were abundant in the Meredosia Districts, but now there are no-

ticeably fewer visible sites (personal communication, 1984).

36

IThe alluvial fans in the Meredosia District, composed of Unit 5 silt

and silt loam, are stratigraphically conformable with the underlying Unit

3. Basal fan sediment is strongly laminated, possibly being deposited in

a shallow lacustrine environment, and may be temporally equivalent with

youngest Unit 3 deposits along the western margin of the Bug Island

Paleochannel. Investigations of other Illinois Valley fans suggest the

bulk of fan deposition in the region occurred after circa 8500 B.P. and

nearly ceased by about 2000 B.P. with noticably decreased rates since

circa 4000 B.P. (Hajic, 1981a; Wiant et al., 1983; Styles, 1984 ). The

preservation of archeological sites in alluvial fan environments is a

common occurrence in the Illinois Valley, and the Meredosia fans are

accorded a high to moderate potential for all cultural periods. Because

of slower depositional rates for the last 4000 years, the potential of

Woodland occupations being fan surface manifestations is greater than the

Archaic. Nevertheless, over a meter of relatively young alluvial fan

deposition (lacking soil development) was recorded in several cores

indicating even the youngest occupations can be buried.

Unit 6, which consists of primarily upland derived alluvium de-

posited as tributary creek overbank deposits is considered to have a

moderate to high potential for containing buried archeological components

as old as about 9800 B.P., or the latest time the Bug Island Paleochannel

could have functioned. Most Unit 6 depositional environments are rela-

tively low energy subsystems and would be conducive to preservation by

burial. Much of Unit 6 deposited by tributaries entering the Meredosia

Village District probably post-dates about 4000 B.P., when fan surfaces

began to stabilize and tributaries incised fan surfaces. Abundant Early

and Middle Woodland sites on similar landscape positions and sediment to

the south suggest Unit 6 deposition nearly ceased by about 2000 B.P. In

similar situations in districts to the south, archeological sites are

often associated with natural levees that rise several feet above local

floodbasins (Hajic, 1981b; 1981c; 1983b).

Unit 7 is correlated with the Hartwell member which is a major

Holocene valley-filling unit in districts to the south (Hajic, 1983b).

The Hartwell was deposited under lacustrine conditions or in a very

37

I

slowly moving fluvial regime. There is little to no potential of buried

cultural deposits in the Hartwell member. There is, however, the possi-

bility of burial of encampments along the lower Bath Terrace scarp as a

result of progressively higher river stages (lake levels?) and Hartwell

member aggradation.

Unit 8 was deposited primarily in swamp and shallow lacustrine

environments occupying depressions in the Bug Island Paleochannel. Accu-

mulation was probably very slow. In districts to the south, the equiva-

lent of this unit, the Buck Lake member, was deposited in the last 3000

years. This may be the case in the Meredosia districts, but the possi-

bility of earlier accumulation exists since the Bug Island channel was

abandoned by about 9800 B.P. Floodbasins and depressional areas, while

seemingly unlikely for habitation, cannot be excluded from burial or

surface site consideration. While perhaps not large in numbers, or size,

specialized camps for activities related to aquatic food procurement are

I a possibility. Equally possible is the lacustrine burial and preserva-

tion of such sites as well as their erosion and destruction by an active-

ly meandering tributary creek.

CONCLUSIONSFor any given study area, the needs for settlement patterning and

predictive modeling of buried and surface site location potentials in

archeological research and cultural resource management are most effi-

ciently and economically served by first modeling the evolutionary histo-

ry of the landscape. Such an analysis includes not only identification

of surficial features and their ages. The location and morphology of

previous landscape features may be deeply buried and have no readily

apparent relationship to the present landscape. The vertical dimension

requires equal emphasis to temporally and spatially define terminal

Wisconsinan and Holocene depositional units and environments, erosional

hiatuses, and paleo-landscapes. In alluvial environments, such a recon-

struction is paramount to establishing the framework which provides the

basis for making sound archeological interpretations.

In the Meredosia Districts, several lithostratigraphic units, which

38

I

comprise large volumes of valley fill, can categorically be excluded from

consideration of buried site potential based upon either their age and/or

environment of deposition. The location and vertical and horizontal

limits of other units that have a high potential for including buried

archeological deposits, such as alluvial fans, have been clearly defined

by subsurface investigation.IBuried and surface site potentials can be evaluated for any poten-

tial borrow areas by using Figure 18 in conjunction with the geomorphic

maps (Figures 4 and 5) and stratigraphic cross-sections (Figures 8-15) of

the Meredosia Districts. A generalized summary for buried site potential

is presented in Figures 19 and 20. Prior to any borrow activities, a

systematic site specific surface survey must still be conducted.IThis investigation is considered a component of the archeological

survey. During subsequent archeological testing and mitigation phases,

specific environments and deposits can, and should, be investigated in

I more detail.

IIIII

: 39

Ip QI

,Ii

I .. - ~-j.

--IA

Fiue1. Etmtd breIit oetasi h eeoiVilgIitit

I4

Aki

r

I 41kA,/

t Figure 20 . stimated buri d site poten i s i th e do aLaeDstit

I 41

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43

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47

I

I

I

I

APPEND)IXA

Core Descriptions

IIII

Note: Weathering zone terminology is after Hallberg, Fenton, and Miller(1979). The terms "oxidized" (0), "deoxidized" (D), and"unoxidized" (U) are stardard terminology based upon certain moistMunsell colors and iron segregations. The weathering zones arealso related to hydrologic conditions such as the length ofsaturated conditions. The second letter refers to unleached (U)and leached (L) condition of the sediments in relation to carbonateminerals. Mottling of the sediment is signified by (M).

I

148

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APPENDIX B

Particle Size and Carbonate Data

1 30

Table B-I. Particle Size and Carbonate Data.

DEPTH CARBONATECORE _(am PARTICLE SIZE (1) MINERALS (T)

Total

Sand Silt Clay Cal- Dolo- Car-I 2mm-63um 63um-2um 2um cite mite bonates

DLC-28 0- 22 65.86 13.88 20.2622- 34 91.85 4.82 3.3334- 46 92.15 5.35 2.5046- 63 94.62 3.57 1.8163- 80 94.09 4.39 1.5280- 98 93.23 5.35 1.4298-110 88.91 8.59 2.50 0 0 0110-123 71.72 20.69 7.59 0 0 0123-139 50.75 36.75 14.00 0 0 0139-155 47.88 27.69 20.19 0 0 0155-168 32.73 8.25 24.48 0 0 0168-183 27.73 44.32 27.95 0 0 0183-199 31.60 42.16 26.24 0 0 0199-202 59.80 24.18 16.62 0 0 0202-211 82.34 13.06 4.60 0 0 0211.224 53.51 29.31 17.18 0 0 0224-240 76.34 15.48 8.18 0 0 0240-260 85.31 9.16 5.53 0 0 0260-280 82.40 7.66 9.94 0 0 0280-300 51.12 35.03 13.85 0 0 0300-320 33.85 48.76 17.39 0 0 0320-340 34.38 47.27 18.45 0 0 0

340-360 38.55 45.40 16.05 0 0 0360-380 37.60 47.67 14.73 0 0 0380-400 4.37 64.05 31.58 0 0 0400-418 57.73 29.44 12.83 0 0 0418-440 86.47 9.27 4.26 0 0 0440-480 92.96 5.08 1.96 0 0 0480-520 94.68 3.95 1.37 0 0.64 0.64520-570 91.25 6.94 1.81 0 2.65 2.65570-620 92.74 1.58 5.68 0.04 2.25 2.29620-670 64.80 28.15 7.05 0.75 8.83 9.58670-720 89.94 7.51 2.55 1.24 6.20 7.44

MLC-19 0- 17 0.97 85.95 13.0817- 32 0.98 83.00 16.02

32- 43 0.43 80.64 18.9343- 57 0.41 79.83 19.7757- 76 0.38 80.54 19.0876- 94 0.24 78.07 21.69

94-107 0.14 75.49 24:37107-120 0.21 T3.71 26.08

131

I

ITable B-1. (continued)

DEPTH CARBONATE-CORE _(a PARTICLE SIZE (1) MINERALS (1)

TotalSand Silt Clay Cal- Dolo- Car-

2mm-63um 63um-2um 2um cite mite bonates

120-132 0.14 76.41 23.45132-152 0.16 75.03 24.81152-169 0.23 71.14 28.63 0 0 0169-186 0.26 76.62 23.12 0 0 0186-210 0.45 85.06 14.49 0 5.01 5.01210-235 0.59 88.69 10.72 0 10.37 10.37235-258 0.45 91.17 8.38 0 9.94 9.94258-269 0.53 79.98 19.49 0 7.95 7.95269-280 0.60 82.17 17.23 0 8.43 8.43

280-288 0.42 90.23 9.35 0 11.71 11.71288-294 1.04 90.98 7.98 0 10.39 10.39294-309 0.52 83.49 15.99 0 11.23 11.23309-325 0.50 84.64 14.86 0 12.07 12.07325-340 0.66 85.00 14.34 0 10.43 10.43

340-360 1.57 66.91 31.52 0 0.64 0.64360-380 0 0.41 0.41380-400 0 0.75 0.75400-420 2.01 67.72 30.78 0 0.75 0.75420-442 2.81 71.98 25.21 0 5.47 5.47442-458 2.41 77.82 19.77 0 9.53 9.53458-478 1.86 87.33 10.81 0 16.19 16.19I 478-498 4.89 84.88 10.23 0 17.26 17.26498-520 4.92 82.99 12.09 0 16.09 16.09520-548 0.77 85.82 13.41 0 15.60 15.60

548-563 4.57 90.78 4.65 0 6.82 6.82563-570 67.64 22.51 9.85 0 7.95 7.95

570-575 74.77 20.58 4.65 0 6.89 6.89

I1

132

APPEN IX C

Outline of Late Wisconsinan and Holocene

Geology of the Lower Illinois River Valley

by

Edwin R. Hajic

133

The purpose of this appendix is twofold: first, to briefly summarize

the geomorphology, stratigraphy and depositional environments, and out-

line a chronology of late Wisconsinan and Holocene events in the lower

Illinois River Valley; and second, to report 21 radiocarbon dates from

levee and drainage districts, 11 of which are previously unreported

(Table C-i). Most descriptive information contained in previous levee and

drainage district reports (Hajic and Hassen, 1980; Hajic, 1981b;c; 1983b;

Hajic and Leigh, this volume) is not repeated here and is deferred to a

more comprehensive summary report now in preparation. Similarly, not all

evidence or supporting agruments are developed here.

The geologic history outlined represents a collection of working

hypotheses. It is certain there will be some refinement or revision of

these ideas as further analyses of the hundreds of collected cores takes

place.

Prior to summarizing geologic events, several salient points re-

garding the general geomorphology of the lower 120 km of the Illinois

Valley which constitutes the project area need to be presented. A varie-

ty of late Wisconsinan and very early Holocene terraces of diverse origin

and morphology are recognized in the lower valley (Figures C-i and C-2).

Two general down-valley trends are evident in all but the Deer Plain

Terrace. Percent valley area occupied by terraces decreases and

sequentially lower terraces progressively drop out (Figures C-I, C-2 and

C-3). The only exception is the Deer Plain Terrace for which the

opposite is true (Rubey, 1952). In the Illinois Valley, the Deer Plain

is characterized by a reverse slope relative to the present Illinois

River. It is broad and featureless except for some dunes at the extreme

southern end. The Bath Terrace (Wanless, 1957; Styles, 1984) is mantled

almost entirely by dunes and has a relatively low slope. In contrast,

the Bluffs Terrace (Styles, 1984; Hajic, 1983b; this report) is

relatively steep and grades up-valley to the Bath (Figure C-3). The

Bluffs is a slightly undulating surface dissected by a broad shallow

paleochannel, the Bug Island Paleochannel. The Bluffs Terrace and

paleochannel abruptly end at a chain of Bath Terrace remnants cutting

diagonally across the va'ley. The Keach School Terrace (Butzer, 1977) is

134

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0 Jacksonville

Explanation

SFioodbaslnSAlluvial Fan/Trib. AlluviumSKeach School Terrace

EM Bluffs TerraceSDeer Plain Terrace....

Bath TerraceEI Bath and older terraces

1 Nutwoodli2 Eldred -.3 H~artwell

Hiliview *

S Meredosla6 Meredosia Lake -7 Koster38 Napoleon Hollow-

attmch figure 2

Figure C-i General geomorphology of the lower Illinois River valley,

north section, east of the Illinois R-iver

137

attach figure 1

00 Carrollton

Figure C-2 General geomorphology of the lower Illinois River valley, south section

138

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Ialmost featureless and exhibits a nearly level surface. It occurs south

of the chain of Bath remnants. Typical Beardstown Terrace (Wanless,

1957) morphology consists of point bars with evidence for scroll bars.

In mapping the Beardstown Terrace, which is identified only in a

restricted reach of the valley above and below Beardstown, Wanless

undoubtedly included some isolated Bath Terrace remnants.ISeveral distinct paleochannel systems are also evident. The Bug

Island Paleochannel (Hajic and Leigh, this volume; Styles, 1984) is a

broad, shallow and straight channel cutting the Bath and Bluffs terraces.

Although largely buried by upland derived deposits, it can be traced from

east of Beardstown south to the diagonal chain of Bath Terrace remnants

where it ends or is abruptly truncated. The Bug Island Paleochannel is

* closely associated with the Bluffs terrace and several channel

bar/islands are considered to be Bluffs remnants. A broad, shallow

anastomosing system, consisting of one to three branches, cuts the Keach

School Terrace and is younger than the Bug Island Paleochannel. This

paleochannel system has common mid-channel bars. Remnants can be traced

at least as far south as Macoupin Creek.

This "multiple channel" system is precursor to an entrenched system

consisting of one to two branches oriented along channel branches of the

anastomosing system, favoring straight reaches, and favoring a course

along the western valley margin. The considerably narrower modern

Illinois River course consists of straight reaches, probably inherited

from this entrenched system, connected by broad bends. It follows the

western valley margin from Valley City to the mouth.

Nearly all preserved paleochannel reaches have been partially re-

worked by yazoo and deferred tributary stream systems.

In sharp contrast to all other Illinois River paleochannel systems

are a series of meanders restricted to the middle Illinois Valley and

best expressed several kilometers northeast of Beardstown. Associated

point and scroll bars were mapped as typical Beardstown Terrace by

Wanless (1957). Styles (1984) has inferred an early Holocene age for

140

this meandering system from its possible lower elevation in relation to

the Keach School Terrace. That the the meanders were produced by the

Sangamon River which presently enters the Illinois Valley just north of

Beardstown remains a possibility.

Figure C-4 schematically summarizes generalized stratigraphy, depo-

sitional environments and episodes of lower Illinois Valley history.

Figure C-5 schematically illustrates in cross-section the stratigraphic

relationships of most lighologic units. It is clear the lower Illinois

record is as much that of a settling basin as a river and outwash stream.

"Kankakee Flood" - 13,300 B.P.

The Bug Island Paleochannel system and the Bath Terrace developed on

Valley train sand and gravel probably in response to the "Kankakee

Flood", described as a large discharge down the Illinois Valley during

construction of the Valparaiso Moraine system sometime between 14,000 and

15,000 B.P. (Willman and Frye, 1970). Although large discharges probably

occurred, there is no indication they were catastrophic. Illinois Valley

discharge was probably augmented by drainage from an initial Glenwood

phase of Lake Chicago between about 14,500 and 13,500 B.P. (Hansel, et

al., in preparation). Oldest radiocarbon dates from the Bug Island

Paleochannel system are 14,590±240 (ISGS-1285) and 14,300±290 B.P. (ISGS-

1263) (Table C-i) and correspond with what possibly is initial Glenwood

phase discharge. The dates also indicate the Bug Island Paleochannel

system and Bath Terrace may just predate about 14,600 B.P. Hansel et al.

indicate from about 13,500 to 13,000 the Chicago Outlet was temporarily

abandoned in favor of lower outlets. This would cause a relative

decrease in Illinois River discharge but the Bug Island Paleochannel

system, at least in part, probably remained functional.

13,300 - 12,000 B.P.

Rubey (1952) suggested the Deer Plain Terrace resulted from blockage

of the mouth of the Illinois Valley by an aggrading Mississippi flood-

plain. Dates of 13,390±190 (ISGS-894) and 13,010±140 B.P. (ISGS-900)

from earliest lacustrine silt below the Deer Plain Terrace indicate

aggradation of the Mississippi Valley effectively dammed the mouth of the

141

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Illinois Valley prior to 13,300 B.P. Clayton (1982) has inferred periods

of aggradation and degradation in the upper Mississippi Valley based upon

glacial, lacustrine, and glaciofluvial events in the southern Agassiz and

western Superior basins. A period of Mississippi Valley aggradation

postulated to have begun prior to 13,500 B.P. and to have continued until

about 12,200 B.P. (Clayton, 1982) agrees with blockage of the Illinois

Valley.

ISGS-894 and ISGS-900 are directly associated with reddish-brown

clay laminae and correspond to a third previously unreported date of

13,360±1OOB.P. (ISGS-875) from uncarbonized coniferous wood and bark

(Hajic, unpublished data). ISGS-875 is also associated with reddish-

brown clay laminae in the Eldred District. The reddish brown clay can be

traced deep in the subsurface below the Deer Plain Terrace (lake plain)

and associated lacustrine clay in the lower Illinois Valley southward to

the lower solum of surface soils on the sediment dam part of the Deer

Plain Terrace thus indicating the majority of Mississippi Valley

aggradation preceeded 13,300 B.P. The two lower Illinois Valley dates

are from unoxidized, ,inleached silt with reddish brown clay, some of the

first sediments accumulating in the lower Illinois Valley in response to

the sediment dam. They mark initiation of a high lake phase (Deer Plain

phase) in the lower valley. Farther upvalley dates of 13,360.t240 (ISGS-

1262) and 13,340±180 B.P.(ISGS-1284) were recovered at or near the

transition from glaciofluvial to lacustrine sediments in the Bug Island

Paleochannel and firmly support lake initiation. Thick sequences of

green moutmorilloritic clay accumulated in the resultant lake until it

drained.

Preserved remnants of the lake plain and sediment dam comprise the

Deer Plain Terrace in the lower Illinois Valley. A date of 12,000±100

B.P. (ISGS-911) is from slackwater and alluvial sediments below a Keach

School Terrace remnant which is inset to a Deer Plain remnant. The date

indicates the Deer Plain Lake phase probably drained just before 12,000

B.P. and the Deer Plain Terrace is older than 12,000 B.P. A thin, firm,

laminated clay unit with pebbles below ISGS-911 records an erosional

interval predating 12,000 B.P. (Hajic, 1981b:85). The erosional episode

144

is probably related to drainage of the Deer Plain lake phase. A date of

12,360±240 (ISGS-1283) was obtained from the lacustrine sediment unit in

the Bug Island Paleochannel. A date of 12,325±75 B.P. (ISGS-415)

(Butzer, 1977; Hajic, 1981a) was recovered from lake margin related

sediments (Hajic, unpublished data). The exact context of ISGS-415 is

questionable, but the two dates narrow the interval of lake drainage and

exposure of the Deer Plain Terrace to between about 12,325 and 12,000

B.P. This interval corresponds with an estimated time of initiation of

Mississippi Valley downcutting of 12,200 (Clayton, 1982) during the

Twocreekan.

In the Mississippi Valley, the deposits below the Deer Plain are

composed of coarser alluvium than in the Illinois Valley (Rubey, 1952).

A wood sample collected from sandy outwash 23 feet below a terrace sur-

face at the mouth of the Missouri River dated to 12,148 B.P. (Flint and

Dewey, 1951). Flint and Dewey (1951) correlated the terrace with the

Festus Terrace of Robertson (1938). Goodfield (1965) suggested the date

could possibly be from below a Deer Plain remnant. If the date is valid,

the remnant is probably not Deer Plain, but rather a younger terrace and

fill indicating a second episode of aggradation in the Mississippi Valley

to levels approaching that of the Deer Plain. At the Sievers South

Quarry section where Deer Plain sediment dam deposits are exposed (Hajic,

unpublished data), a second, lower terrace is preserved. This unnamed

terrace verifies an erosional episode between Deer Plain formation and a

second episode of Mississippi Valley aggradation. A highly dynamic,

fluctuating Mississippi is implied.

Flock (1984) names and describes surficial sediments of the Savanna

Terrace in the Mississippi Valley extending from Pepin County, Wisconsin

to Jackson County, Illinois. He correlates the Deer Plain as part of the

Savanna Terrace, and in fact Rubey (1952) originally mapped the Deer

Plain in both Mississippi and Illinois Valleys. Flock characterized the

upper 1 to 3 meters of Savanna Terrace sediment as being dominated by red

and gray clay originating from Lake Superior sources and lake basin(s)

farther to the west, respectively. These are the same deposits traced

deep into the Illinois Valley subsurface. Interpreting Hajic's dates of

145

13,360± 100 (ISGS-875), 13,390±190 (ISGS-894) and 13,010±140 B.P. (ISGS-

900), and Goodfield's date of 12,148±700 B.P., he concluded the SavannaTerrace formed sometime between 13,000 and 9500 B.P.

Flock considers the red and gray clays to be deposited during

flooding of either early Lake Superior sometime between 12,000 and 11,000

B.P., Lake Grantsberg sometime between 12,700 and 11,800 B.P. or/and Lake

Agassiz sometime after about 12,000 B.P. In view of earlier discussions,

these ages, with possible exception of early Lake Grantsberg ages, are

probably too young for the Savanna Terrace and associated reddish brown

clay. They are all certainly too young for the considerable thickness of

Deer Plain (Savanna Terrace) forming sediments below the surficial

reddish-brown clay zone at the mouth of the Illinois Valley.

Elevations of the Illinois Valley mouth sediment dam and documented

wave-cut scarps preserved beneath valley margin alluvial fans in the

Illinois Valley, along with soil-geomorphic relationships on the Deer

Plain Terrace, indicate lake levels were high enough to inundate the

entire lower valley and considerable reaches of most tributary streams

(Figure C-3).

During this Deer Plain lake phase, the Illinois River, when active,

would have been terminating at the head of the lake, probably north of

Beardstown. Hansel et al. (in preparation) indicate the Chicago Outlet

was operating when Glacial Lake Chicago in the Michigan basin was at the

Glenwood level probably between 14,500 and 15,500 B.P. and again between

13,000 and 12,200 B.P. There would have been relatively reduced dis-

charge down the Illinois Valley as the Deer Plain sediment dam formed.

Stratified lacustrine fill in the Bug Island Paleochannel may in part

reflect distal alluvial fan delta deposition. Terrace elevations are

such that surficial sediments associated with the Bath or Bluffs Terrace

may also be lacustrine in origin (Figure C-3).

The existance of a lake in the lower to mid-Illinois Valley from

after 13,300 B.P. to about 12,325 B.P. indicates conditions unfavorable

for deposition of loess with an Illinois Valley source during this

146

interval and probably Mississippi Valley source as well. The time range

is compatible with estimates on terminal loess deposition for the region

(McKay, 1977).

12,000 - 9,800 B.P.

A detailed chronology of Illinois Valley events for the period

following drainage of the Deer Plain lake phase until about 10,600 B.P.

is elusive. It is probably characterized by fluctuating intermittant

glaciofluvial, fluvial and lacustrine regimes with only little indication

of deposition. Where sedime; ts from this interval have been preserved,

such as in the Bug Island Paleochannel, they record a varied history of

slackwater deposition with only occasional fluvial input. There is no

indication lake levels approached those of the Deer Plain lake phase.

Exposure of a sandy alluvial plain (Bug Island Paleochannel system)

is evidenced by the migration of dunes onto Bath Terrace remnants shortly

after 10,900 B.P. Radiocarbon dates of 10,900±80 (ISGS-1169) and

11,070±80 B.P. (ISGS-1277) were obtained from wood samples from a woody

peat and underlying fine sandy loam, respectively, which were overlain by

dunes and underlain probably by reworked valley train material. The

presence of fluvially reworked dunes or absence of dunes on the Bluffs

Terrace suggests it may be younger than about 10,900 B.P.

By about 10,600 B.P. and perhaps slightly earlier, another lake

phase was initiated in the lower Illinois Valley and continued into the

very earliest Holocene, about 9800 B.P. The lake plain which was exposed

around the latter date is the Keach School Terrace.

Styles (1984) has recovered organic matter from slackwater sediments

at the mouth of Napoleon Hollow which dated 9950±260 (ISGS-819). The

sample was above the Keach School Terrace elevation indicating the Keach

School lake phase lasted at least through 9950 B.P. Similarly, Hajic

(1983a; in preparation) obtained a wood sample from a corresponding

slackwater unit in Campbell Hollow on the east side of the Illinois

Valley. The material yielded a date of 10,460±220 B.P. (ISGS-989). The

147

Keach School Terrace is incised by an early meander belt of Mauvaise

Terre Creek which was contemporaneous with the "multiple channel" system

of the Illinois River. Wood from basal slackwater sediment filling the

meander belt dated to 9750±70 B.P. (ISGS-1264) (Table C-I) indicating

Keach School Terrace formation predates this age.

Keach School lake phase related deposits include a surface veneer of

interstratified silt, silty sand and sand on the Keach School Terrace.

At several locations the individual fine textured beds were tracable for

hundreds of feet (Hajic, unpublished data). Basal laminated alluvial fan

silt deposits occurring in the south segment of the preserved Bug Island

Paleochannel probably date to this interval. They reflect either rapid

alluvial fan accumulation or alluvial fan delta deposition during

temporarily higher lake level stands.

A probable shoreline is recorded along the northern extent of the

Keach School Terrace at the diagonal chain of Bath Terrace remnants. The

Bug Island Paleochannel is either truncated by this Keach School lake

phase or at least in part contemporaneous with it because the

paleochannel appears to abruptly terminate on the north side of the chain

of Bath Terrace remnants.

Changes in relative amounts of discharge entering the lower valley

during this interval can be inferred from work in the Lake Michigan Basin

by Hansel et al. (in preparation). During the Two Creeks low lake phase

in the Lake Michigan Basin, beginning about 12,000 B.P., the Chicago

Outlet was temporarily abandoned. Considerably reduced discharge would

have been entering the lower Illinois Valley. An increase in discharge

would have accompanied reactivation of the Chicago Outlet at about 11,800

B.P. with establishment of the Calumet Lake phase. Shortly before 11,000

B.P. the Chicago Outlet was abandoned again as deglaciation opened

outlets to the east and Illinois Valley discharge decreased. It is

shortly after 11,000 B.P. that an episode of dune formation is evident in

the lower Illinois Valley.

During the Twocreekan interval the Mississippi River is inferred to

148

have been downcutting (Clayton, 1982). After a brief period of aggrada-

tion, another interval of downcutting occurred until about 10,800 B.P.

The beginning of the aggradational episode at this time may correspond

with initiation of the Keach School lake phase. According to Clayton and

Moran (1982) and Clayton (1982), the Marquette advance of the Superior

Lobe was probably responsible for blocking eastern outlets of Lake

Aggassiz initiating the Emerson Phase in that basin at 9900 B.P. With

blockage, Lake Aggassiz drained into the Mississippi River via the Minne-

sota River. The episode of Mississippi Valley downcutting which this

chain of events initiated caused the Keach School lake phase to drain and

the Illinois River to downcut rapidly. Lake drainage probably caused the

streamlining of several Bath Terrace remnants along the south and east

part of the diagonal chain of Bath remnants.

9800 - 7000 B.P.

Initial downcutting occurred in an anastomosing pattern of 1 to 2,

and possibly 3, channels which are best expressed immediately north and

south of highway U.S. 36. Morphology of this channel system may have been

influenced in part by Keach School lake drainage. This channel system

was only temporary and with continued rapid downcutting some branches

where abandoned and preserved. There is some evidence to suggest the

preserved bed of this anastomosing system was subaerially exposed for an

undetermined period of time. An early Archaic site, now buried by late

Holocene deposits, is preserved on this surface in the Eldred District

and there are some indications of associated soil development (Hassen and

Hajic, 1983). This buried surface, which is most extensive south of the

Hillview District, is informally referred to as the Columbiana surface.

Ultimately, downcutting was on the order of at least 15.2 m for

channel bases. River stage fluctuation is not yet clear. There is no

evidence of subaerial exposure of Holocene surfaces (i.e., floodplain)

greater than 5 to 6 m below present floodbasins. Near-surface sediments

below the Keach School Terrace indicate subsequent Holocene river (and

flood) and lake stages did not eclipse Keach School elevations to leave a

recognizable overbank deposit. Apparently all fluvial and lacustrine

events post-dating the very early Holocene downcutting were confined to

149

the incised channels defined by the Columbiana, Keach School and older

terrace margins, and the bedrock valley walls.

Maximum downcutting was accompoished by about 9500 B.P. and a

probable lake phase, restricted to incised channels, ensued for an

unknown length of time. Radiocarbon dates on wood from slackwater(?)

clay at relatively low elevations are 9480±130 (ISGS-1135) and 9300±150

(ISGS-1122) (Table C-i).

The period between 9000 and 7000 B.P. is not well known and there

are only several areas where deposits from this interval are recognized

at all. The present general location of the Illinois River is currently

viewed as the location of the main channel of the several utilized during

downcutting with only several areas of exception. This view tends to be

supported by Corps of Engineers boring records along artificial Illinois

River levees which indicate the greatest depths of fine textured

sediments found in the valley. The Illinois River, when functioning as

such, has apparently assumed a general position along the western valley

margin and has not varied significantly throughout the Holocene. Largely

negative evidence for this is derived from the slackwater Hartwell member

of the Cahokia Alluvium. The Hartwell, filling paleochannels incised

during the initial Holocene and deposited between about 6000 and 3000

B.P., constitutes the bulk of Holocene valley fill, yet it is a very

uniform deposit for considerable thickness at any given location.

Texturally and structurally it exhibits little, if any, indication of

alluvial channel, bar, natural levee, or floodplain facies.

7000 - 3000 B.P.

Infilling of paleochannels was possibly underway by at least around

7000 B.P. as indicated by stratigraphic contexts of a burled Archaic

horizon at the Napoleon Hollow Site (Styles, 1984). Sometime before

6400 B.P. the Illinois River clearly established its course along the

western side of the valley south of the Hillview district and is evi-

denced by remnants of a well de-eloped natural levee system. The Quasar

site, a shallowly buried Archaic horizon within these natural levee

deposits, yielded a date of 6320±90 (ISGS-1278) (Table C-i). In downcut

150

paleochannel segments abandoned by Illinois River straightening and

channel definition by first subaqueous, then subaerial natural levee

formation, Hartwell lacustrine or nearly slackwater conditions were

established by 5700±140 B.P. (ISGS-930) and most likely continued beyond

3650±70 B.P. (ISGS-903) (Table C-I). Hartwell deposition occurred in

relatively deep backwaters. Deposition was relatively rapid and

paleochannels infilled to several meters below the present floodplain

surface. Structure of lower soil horizons is preserved at the top of the

Hartwell indicating an emergent floodplain.

3000 B.P. - 1920's

The presettlem-nt general structure of floodbasins and natural

levees evolved during the 500 years predating about 2500 B.P. Around

3000 B.P. a primarily erosional eposide, referred to as the McFain event,

effectively planed the Hartwell surface, reworked terrace margins, and

scoured portions of the Columbiana surface. The associated McFain member

probably represents a lag resulting from either a large Illinois River

discharge or active yazoo streams meandering across the emergent

floodplain. A radiocarbon date of 2890±75 B.P. (ISGS-143) on shell

(Coleman, 1974) was obtained from deposits interpreted to be the McFain.

Buck Lake member deposition followed in shallow backwater lakes,

possibly intermittent, as a floodbasin aetwork of coelescing tributary

creeks rapidly built a natural levee system. Slow aggradation occurred

in floodbasins. The Illinois River went through minor redefinitions of

its channel position and there is evidence to suggest a second natural

levee set, finer textured than the first, rapidly developed during this

interval. Early Woodland settlements are common on the natural levees

indicating they were well established by about 2500 B.P. Dates of

2420±70 B.P. (ISGS-1120) and 1980±80 B.P. (ISGS-1084) were recovered from

the bottom and top respectively of fill from one of the floodbasin yazoo

stream channels (Table C-I). The dates may indicate a rough range for

the infilling and final deactivation of the yazoo system, but clearly

more dates will be necessary.

The Illinois River has maintained its west side channel with little

151

modification throughout the last 2500 years as indicated by Early

Woodland settlements on Illinois River natural levees (Farnsworth, 1976;

Butzer, 1977).

1

I

I5

APPENDIX D

Scope of Work

153

CULTURAL RESOURCE SURVEY OF SELECTS) PORTIONS OF THEHEREDOSIA AND MEREDOSIA LAK DRAINAGE AND LEVEE DISTRICTS

SCOPE OF WORK

1. Statement of Work. The work to be accomplished by the Contractorconsists of furnishing all labor, supplies, materials, plant andequipment necessary to perform a Cultural Resource Survey of selectedportions of the Meredosia and Meredosia Lake Drainage and LeveeDistricts, Scott, Cass and Morgan Counties, Illinois, and furnish awritten report thereon as set forth in the Scope of Work.2. Location and Descriotion of Study Area. The project area is situatedin the Illinois River floodplain between river miles 65.0-72.0 (MeredosiaD & LD) and 72.0-79.0 (Meredosia Lake D & LD) in Scott, Cass and MorganCounties, Illinois. The total area to be physically surveyed consists of3140 acres and represents approximately a 20% sample of the entire areacontained within the two districts (15,725 acres).

3.1 Genera1. The Contractor is responsible forthe formulation,justification and conduct of the study to include the design andexecution of all survey methods and procedures as well as thepresentation of the study results unless otherwise set forth in thisScope of Work.

3.2 Sample Design. The survey will be structured so as toinvestigate a representative portion of each topographic andphysiographic zone (i.e., ridges, terraces, etc.). As a result, theContractor will restrict his investigation to a 20% stratified randomsample of appropriately selected zones. Before initiating the fieldwork,the Contractor will provide the Contracting Officer's Representative withmaps showing the sample units selected and with a narrative describinghow the units were chosen and describing the research goals andobjectives, as these relate to larger questions about Illinois RiverValley prehistory (i.e., a "research design"). The Contracting Officer'sRepresentative will comment (see Paragraph 6.1).

3.3 Principal Informant Interviews. Principal Informant Inter-views constitute preliminary surveys based on verbal descriptions of sitelocations. The Contractor will contact amateur archaeologists and col-lectors within the region in an attempt to identify the location ofpreviously known archaeological or historic sites within the Meredosiaand Meredosia Lake Drainage and Levee Districts. On-site analysis shallconsist only of a visual confirmation of the verbal description.

3.4 Pedestrian Survey. The Pedestrian Survey will consist of anintensive on-the-ground survey of each sample unit, sufficient todetermine the number and extent of cultural resources within each unit.This process will include one complete surface collection at eachidentified site.

3.5 Lab Procedures. Artifacts collected during survey activitiesshall be washed, permanently labeled and catalogued according to standardlab procedures. These collections shall be analyzed in an attempt todetermine each site's temporal affiliation and horizontal surfacedistribution. All artifacts will be separated into various general

154

categories, then subdivided into smaller, functional and stylisticcategories. These distributions shall be quantitatively assessed in aprofessional, concise manner.

3.6 Curation of Material. The report shall contain a statementindicating the exact location of all materials and records resulting fromthis contract work. This statement shall include at a minimum, the nameand address of the curatorial building, the storage room number, and ifpossible, the rack, shelf or cabinet number where this material isstored. Containers in which artifacts are stored shall be clearlylabeled "Property of the U.S. Government, St. Louis District, Corps ofEngineers."4. Final genort. The Contractor shall prepare a written report whichpresents and interprets survey results, and describes in detail datacollection techniques. A discussion of each site located, its culturalaffiliation and artifact assemblage, as well as their relation to othersites found during the survey shall be presented in the text of thereport. These data shall then be compared to other previously reportedsites in the Illinois River Valley and surrounding areas in order toplace the results of this study into regional context. In addition theFinal Report shall include the following:

a. U.T.M. coordinates of each site, detailed site-specificdescriptions, locational data and maps attached as appendix to the FinalReport.

b. Maps which accurately define site locations, site numbers,areas surveyed, and ground cover conditions as well as other pertinentdata. These data must be recorded on U.S.G.S. topos (scale 1:24000)although other maps may be used as well.

c. No hand lettering is acceptable other than that necessary torecord data on base maps.

d. Oversized maps will be folded and included in a pocket inthe back of the appropriate report section or appendix.

e. A full set of reproducible maps, plates and drawings.f. Black and white prints (half-tones) of diagnostic and

functionally significant artifacts will be incorporated into the reportbody or attached as appendix.

g. A photographic log of annotated 35mm slides, showing eachphase of lab and fieldwork in progress shall be included with FinalReport original.

h. An abstract not to exceed one typewritten page.i. Completed site forms shall be submitted for each site

identified during these surveying activities.

5. Permits and Rights of Entry. Rights of Entry upon work sites forperformance of work under this contract shall be obtained by theContractor. The Contractor shall obtain the necessary approval to enteron any private property and to permanently remove any artifacts recoveredduring subsequent surveying activities. Should access to certainportions of this project area referenced in Paragraph 2 above be denied,the actual amount of this order will be decreased in an amount equal tothe percentage of difference between the original required acreage andthat acreage actually surveyed.

155

6. Schedule of Work6.1 Research Design. Research Design (see Paragraph 3.2) shall be

submitted to the Contracting Officer's Representative within 20 days ofthe date of the delivery order. The Contracting Officer's representativewill review and comment within 7 calendar days of receipt of ResearchDesign.

6.2 F. All fieldwork related to this item shall becompleted within 200 days after the date of the delivery order.

6.3 Draft Report. Five copies of the draft report shall besubmitted by the Contractor to the Contracting Officer's Representativewithin 90 days after fieldwork is completed. Government representativeswill review the report for compliance with the requirements of thecontract and will return the preliminary report, together with anywritten comments thereon, which may require changes in the report, to theContractor within 50 calendar days after its receipt. The report shallbe organized in a manner consistent with the St. Louis District reportformat guidelines. The title page shall be organized in a mannerconsistent with the St. Louis District title page format guides.

6.4 Finl Coy=. While the St. Louis District is reviewing thecontractor's draft report, the St. Louis District will prepare reportcovers for the final report and will forward these to the Contractor withdraft comments. The Contractor shall be responsible for binding thefinal report in these covers, using Plastic Spiral Binding.

6.5 FinReo The Contractor shall submit 30 bound copies ofthe Final Report, including the original copies signed by the principleinvestigator, to the Government within 30 days after the Contractorreceives the St. Louis Districts written comments. A set ofreproducibles of all drawings, plates and other graphics, including siteforms, shall be furnished at the time of submission of the Final Report.7. Exesin, In the event these schedules are exceeded due to causesbeyond the control and without fault or negligence of the Contractor,this delivery order will be modified in writing, and the contractcompletion date will be extended one calendar day for each calendar dayof delay.

156

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