Guide leaflet, geological science field trip, Greenup area : Cumberland County, Casey, Kansas, Oakland and Toledo quadrangles

State of Illinois
Department of Registration and Education
STATE GEOLOGICAL SIRVEY DIVISION
John Co Frye, Chief

EAKTH SCIENCE FIELD RIP

C UMBER LAND COUNTY

CASEY, KANSAS, OAKLAND, AND TOLEDO QUADRANGLES

Leaders
George M. Wilson and I. Edgar Cdom
Urbana, Illinois
September 25, 1959

GUIDE LEAFLET 1959~E HOST? CUMBERLAND COUNTY HIGH SCHOOL

LIBRARY.

CBEENUP EARTH SCIENCE FIELD TRIP

ITINERARY

OoO OoO Northeast corner of the Cumberland High School Yard, at the
T-road south from Route 121.

CAUTION in entering Route 121. Turn left.

.1 61 Turn right. Entering a crushed rock road* For the next several
miles the upland surface is on the Illinoian till plain. The
Illinoian was the third of the glacial stages in North America
durinc the Pleistocene and was the most extensive in Illinois.

.2 ,3 Turn right.

.1 .ii Turn left. The Illinoian glacier reached as far south as

Equality, Illinois, as far southwest as six or seven miles south
cf Carbondale and reached to the bluffs of the Mississippi
River. The Illinoian till plain is characterized by flatnsss
of the upland surfaces though the till plain has besn
considerably dissected by erosion from streams that have
developed since Illinoian time, especially in the Wisconsin
stage of glaciation and following.

.8 lo2 CAUTION crossroads.

.9 201 Turn right (east) at T-road south*

•6 2o7 Turn left (nc^th). By referring to your map you will note

that we are paralleling the north- r^uth couise of the Erah^rrass
River (pronounced Embraw), As we progrecs northward in this
route we will find till exposures which have heretofore been
called Illinc tan but would appear at the present tima to be of
fluviatlle origin and not Illinoian, possibly pro-¥i?consin.

«9 3.6 STOP 1

Ft, in.

Zone A A gray timber soil, with finely
divided humic material

Zone B-l A brownish gray sub soil

B-2 Brown-reddish brown, plainly
showing the redeposition of
the iron-bearing minerals that
have been leached from Zone A and B-l.

Zone C-l Glacial till oxidized and not leached
and effervesces freely with acid.

- 2 -

Ft, In0

C2- Glacial till unaltered-gray; with
several thin sand lenses showing
throughout the entire outcrop; shows
faint traces of laminations, 10

Before we can properly approach our field trip today we must
give thought to the problem of where and how most of the soils
of Illinois were derived^ They were brought to Illinois as
glacial drift and have developed in place as soils.

Tens and hundreds of thousands of years ago most of Illinois,
together with most of northern Worth America, was covered by
huge ice-sheets or glaciers. These glaciers expanded from
centers in what is now eastern Canada, They developed when for
some reason not yet determined the mean annual temperatures in
the region were somewhat lower than now, so that not all of the
snow that fell during the winters was melted during the summers.
The snow residues accumulated year after year until they became
a sheet of ice so thick that as a result of its weight the
lowermost part began to flow outward, carrying with it the soil
and rocks on which it rested and over which it moved. The
process continued until the glacier extended into our country
as far south as Missouri and Ohio riverso

Moderation of temperatures halted the glacier c For a while
the melting of the ice balanced its accumulation and expansion,
so that its margin remained stationary. Later the melting
exceeded the accumulation and expansion, and the ice front
gradually melted back until the glacier disappeared entirely.

As the glacier melted, all of the soil and rocks which it had
picked up as it advanced were released. Some of this material
or drift was deposited in place as the ice melted. Such material
consists of a thorough mixture. -of all kinds and sizes of rocks
and is known as till. Some of the glacial drift was washed out
with the melt-waters. The coarsest outwash material was
deposited nearest the ice-front and gradually finer material
farther away0 The finest clay may have been carried all the
way to the ocean. Where the outwash material was spread widely
in front of the glacier it forms an outwash°plain; where it was
restricted to the river valleys it forms what are called valley»
trains.

At times, especially in the winters, the outwash-plains and
valley-trains were exposed as the melt-waters subsided, the
wind picked up silt and fine sand from their surfaces, blew it
across the country, and dropped it to form deposits of what is
known as loess. Glacial loess mantles most of Illinoisc. Near
the large river valleys it may be as much as 60 or 80 feet
thick. Far from the valleys it may be measured only in inches,
if it can be identified at all.

Digitized by the Internet Archive

in 2012 with funding from

University of Illinois Urbana-Champaign

http://archive.org/details/guideleaflet59wils

. 3 -

It is now commonly known that there were four major peHods
of glaciation during the Pleistocene or Great Ice Age (see
accompanying table), and that between each pair there was a
long interglacial period in which conditions were as they are
today* It is also commonly known that during each major
glaciation there were a number of retreats and readvancesa
This was particularly true during the last or Wisconsin glacial
stage •

The Greenup area was invaded certainly by the glaciers
during the last three - Kansan, Illinoian, and Wisconsin -
glacial stages, because glacial drift of these ages may be
found in the region. Probably the region was also invaded
by the Nebraskan or oldest glacier, although no materials
positively of Nebraskan age have been identified*

The position of the ice-front at each advance of the glacier
is usually marked by a ridge of till or moraine. The moraine
represents the accumulation of drift at the ice-martin while
the advance and melting were essentially in balance, when more
and more material was being brought to the edge of the advancing
ice* When melting exceeded advance, so that the ice-front
retreated, the resulting drift deposits form a drift-plain or
till-plain^ whose surface may be almost level or* moitf or less
billowy* Fifty feet north of this particular outcrop^ is a
very gravelly zone near the top of the soil profile in position
of B2e From the standpoint of an erosion cycle this section of
the country is in a very youthful stage of erosion.

>6 Uo2 Crossroads. In general the till in this section of the country
is comparatively thin*.

>5 hoi Oftentimes the streams are bottomed in bedrock as we note here,
with an average thickness of glacial drift in this section of
35 or UO feet.

• 5 5.2 Crossroads. With an earlier publication, written by Dr. M. M.
Leighton and Paul MacClintock, the till here was identified as
Illinoian with underlying older tills. Due to the slumping in
this section of the country we have been unable to find the
exposure along the roadside.

>7 5*° Note the thickness of the soil zone* The B Zone is perhaps 5
feet thick and grades imperceptibly into the C Zone, but note
the faint traces of laminations in Zone C.

,7 6.6 At T-road south, turn right (east).

,2 6.8 Wote the farm buildings on the left and the terrace upon which
the buildings are built. We are entering the flood plain of
the Embarrass River.

.1*

7.8

a

7.9

ol

8.0

a

8.1

-ll -

,3 7.1 Crossing the Embarrass River, note the Pennsylvanian rocks
outcropping on the east bank of the river.

•1 7.2 Ascend hill and turn left, leaving the valley of the Embarrass.
This is the highest level terrace developed on the Embarrass.

.2 7*U Turn right (east). Note gray till capped with reddish brown
sandy soil among the hills on the far left.

This is a middle terrace level.

This is the lowest terrace level.

CAUTION rough bridge.

STOP 2. Stop 2 is a gravel pit owned by the Casey Stone
Company, developed in the Embarrass terrace. The gravel here
is some 75 feet in thickness. From the present point of
view, I would suggest that the terrace developed as a pro-
Shelbyville deposit or in the earliest stage of the Shelbyville
when great quantities of meltwaters entered the Embarrass Valley.
With the development of the valley train in the Embarrass Valley
the gravel carried by the great quantities of water was laid
down because of the overloading of the streams. Then with the
development of the later stages of the Shelbyville ice and the
succeeding stages of the Cerro Gordo, West Ridge, Champaign,
Urbana, and other moraines, the Embarrass was re-cut into these
terraces, with the resulting two lower terrace levels, before
reaching the valley of the Embarrass.

8.5 Note the gravelly soil on the left, reaching nearly to the
upland.

SfcOpo CAUTION in entering Route 130. Turn right (south).

Note the thin soil profile on the Illinoian till upland on the
righto

Note the thin profile of Zone A and B.

Note the gravelly soil on the east side of the highway*

Entering Hurricane Creek Valleye Hurricane Creek was a sluice-
way for the effluent waters of the Shelbyville stage of
glaciation and as a result considerable quantities of gravel
have been deposited along this stream.

•7 12*3 Slow, Turn left (east)o

»3 12 o 6 Note the gravelly soil on the left as well as thin lenses of
gravel. The soil here is calcareous to within 3 feet of the
surface of the earth.

• 7

9.2

o2

9.1

• 7

10.1

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11,2

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11.6

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- 5 -

.7 13«3 T-road north. Continue ahead.

One of the most striking characteristics of the Illinoian till
plain is the comparative flatness of the upland surface. This,
however, may be slightly altered by the presence of a thin
veneer of Wisconsin drift. The statement still holds true
that the IllinoiiaR till plain upland surface is definitely
flat.

1.0 1U«3 CAUTION. Rough bridge. Load limit, $ tons.

.1 1U-U STOP 3.

Soil Profile in Illinoian Till

Ft. In.
Zone A Timber soil - gray with finely

divided, humic material 7

Zone B-l Oxidized, leached brown - olive 1 6

Zone B-2 Brown - reddish brown 1 6

Zosae C-l Deeply oxidized and non-
calcareous till, reddish brown 3

Zone C-2 Oxidized and quite calcareous

till 2 plus

The soil profile here is sufficiently far from the
sluiceways of the Shelbyville that there is a normal soil
profile development.

«5> 111* 9 T-road north. Continue ahead (east).

.6 15.5 CAUTION. Crossroads. Continue ahead (east).

1.0 16.$ Slow. Turn left (north).

.8 17*3 Crossroads. Turn right (east).

.8 18.1 We are in the Siggins Pool, one of the early oil fields of
Illinois, which was developed in sand of Pennsylvanian age and
has produced since about 1905. The primary production has
given about 10,000 barrels per acre for the center portion of
the field. Since the development of secondary recovery
techniques, which were introduced to Illinois by the late Dr.
Frederick Squires, a second crop of oil has been obtained.
This has resulted in the production of more than 10,000
barrels per acre for a portion of the pool. The more
productive part is the zone where the sand is thickest and
has the best interconnected porosity and permeability.

•5 18.6 Slow. T-road west. Turn left (north).

• 1 1-

- 6 -

STOP h* Turn right for discussion of the Siggins Pool.

.£ 19.1 Turn left (north).

What remains for the third crop of oil will remain to be

developed in later years. Whether or not the addition of

heat and fire will drive out another crop, remains to be proven.

•U 19.5 Turn left (west)8

Note that the pump jacks are quite small, the reason being
that the wells are comparatively shallow. Since the beginning
of the water flooding operations some 50,000,000 barrels of
water have been injected into this oil field by the Forest Oil
Corporation. The Forest Oil Corporation is one of the operators
in this field, and other interests have injected water also.

.5 20.0 Slow. Turn right.

.6 20.6 Turn left (west).

.k 21.0 CAUTION. Rough bridge.

.6 21 « 6 Crossroads. CAUTION.

1.0 22.6 CAPTION., Crossroads at Union Center.

i.O 23.6 CAUTION. Crossroads.

.6 2i|.2 Note the sandy soil in the roadcut on the right and left.

.2 2ii.li STOP £.

At this stop we have a dune sand perched on top of the hill.
This dune sand is of Wisconsin age and ranges from nothing to
five feet in thickness. Beneath this is Zone A, which is
loessal in appearance, is buff to tan and is perhaps 3 feet
thick. Zone B-l is about 2 feet thick. Zone B-2 is brown
weathered and oxidized non- calcareous throughout^ that is,
Zone A, B-l and B-2. The lower portion of B-2 is also non-
calcareous, oxidized, and leached. B-2 is about 7 feet in
thickness 0 Some 150» further west is an interesting development
in that the soil here is quite gravelly and is calcareous to
within 3 feet of the surface. This development is due to a
terrace development in the Embarrass Valley and is not of
Illinoian age as were the previous deposits but is of
Wisconsin age.

To the north, only a short distance, is a gravel operation
developed in a lower terrace level on the Embarrass Valley.

<>2 2U,6 Crossing Hurricane Creek,

The till profile is even better than in the exposure
and reads thus:

- 7 -

F t o In*

Zone A Gray and slightly humic timber soil 7

Zone B-l Developed in the Wisconsin sand 3

Buried Illinoian Soil

Zone A Brown, sticky, fine, oxidized

leached 6-7

Zone B-l Buff-colored, oxidized, leached 3

Zone B-2 Concentration of quartz pebbles
in upper portion, oxidized,
leached $

Zone C-l Exposed at bottom of bluff,

effervesces freely with acid. 5

.9 25»3> Slow. STOP. Turn right, entering Route 130.

1.0 26.5? Notice the hills dead ahead some six or seven miles, This is
the Shelbyville Moraine of the Wisconsin stags of glaciation.

.7 27o2 We are rising imperceptibly toward the moraine.

.8 2&0 We are rising on the normal slope of the Shelbyville Moraine.

1.3 29.3 Slow. Turn left, entering Fox Ridge State Park.

.2 29*$ Y road, hold to the right.

.9 30.U LUXH STOP 6. At the pavilion of the Fox Ridgs State Park.
When lunch is over make sure that the lunch sacks are placed
in waste receptacles. Retrace the same road to Route 130.

1„2 31.6 CAUTION on entering Route 130. Turn left (north).

d 31.7 Uct© the gravolly fcfia oa the s?2$&t,

.2 31*9 We are climbing the front of the Shelbyville moraine, which in
this section of the country has three crests, indicating the
probability of three separate advances of the Shelbyville ice*

2.7 3U» 6 Crest of the moraine. We are going down the back slope of the
Shelbyville entering the Embarrass Valley.

1»0 35*6 Gravel pit on the right developed in a terracs in the
Embarrass Valley*

oh 36.0 Cross the Embarrass River 0

- 8 -

Slow. Turn right, entering Charleston City Park.

.1 36.1 Turn right.

.2 36.3 STOP 7 for visit to the Pennsylvanian plant fossil-bearing
shales and siltstones below the dam on the Embarrass.
The section here is, beginning at the top, terrace gravel some
seven or eight feet in thickness, followed by 15 feet of
brownish to olive-colored shale, which is filled with ironstone
concretions. After a slight unconformity, gray shale, medium
to coarse-grained, unconformably overlies the sandstone, which
has an irregular upper surface. The sandstone is estimated to
be 1$ feet in thickness.

At the beginning of Pennsylvanian time, some 25>0 million
years ago, conditions changed when high mountains began to rise
along the Atlantic Coast. Toward the west, in Illinois and
elsewhere, was a low hot swampy plain, somewhat resembling the
present Amazon Basin. Across the plain, rivers from the eastern
mountains wandered toward the sea which lay off in Nebraska,
Kansas, and Oklahoma,, As the lowland sank, the sea from time
to time extended eastward to deposit marine limestone or
fossiliferous shale. At other times there were vast jungle
swamps in which luxuriant vegetation accumulated as half-rotten,
peat-like masses. But most of the time the lowland was
occupied by rivers, shallow lakes, and bayou;-: in which mud and
sand, washed out from the mountains, was deposited* In bime,
thousands of feet of sediments pf.led up, and the pressure of
this great weight of mud and sand helped to compress the peat
to coal with a repetition of similar sequences.

This succession of different kinds of strata is repeated in
much the same sequence some 3>0 times where the Pennsylvanian
(Coal Measures) rocks are thickest. Each succession of
Pennsylvanian rocks is called a cyclothem (see attached chart).

These different strata indicate many rapid changes of
environment which took place repeatedly during the Pennsylvanian
period. At that time rivers were bringing sediments from the
north and east, possibly from as far auay as the present
Atlantic coast. The ocean lay to the west and south* The
country in between, which is now the Middle West, was a lew
flat swampy area in which the sediments were being deposited.
There is no area on earth today that has conditions like those
that existed during Coal Measures time.

The plants and trees that grew at that time were very
luxuriant. As the plants fell into the swampy waters they were
partially preserved, buried by later sediments, and converted
into coal. Some times the sediments were fine silts and clays,
and at still other times the sea covered the area and left
marine fossils.

Continue ahead, following the black- top route through the park*

- 9 -

.5 36,8 CAUTION in descending hill. Shift into lower gear0 Turn right.

.2 37.0 STOP. CAUTION in re-entering Route 130. Turn left.

.1 37.1 Cross Embarrass River.

1.3 38.JU Turn left on the Hut ton Road.

.8 39.2 Slow. Turn left to enter East-West road. This road follows
the crest of the second lobe of the Shelbyville Moraine.

3.0 1*2.2 The outermost lobe of the Shelbyville Moraine is on the far
right.

•1* 1*2.6 Crossroads. The building on the southwest corner is a barn of
log construction, dating back to the latter part of the 19th
centuryo

♦ 5 1*3.1 Here is an excellent view of the southernmost lobe of the

Shelbyville Moraine. We are traveling on the middle ridge.

STOP 8. Here the middle lobe of the Shelbyville ice has over-
ridden the outer lobe. Here we have an excellent view of the
Illinoian till plain to the south. The topographic difference
between the top of the ridge here and the Illinoian till plain
is 110 feet.

1.3 1*1**1* Turn left.

.1 1*1*»5 Turn right.

.1 1*1*«6 A view of the second crest of the Shelbyville Moraine is

afforded to the north, some mile and a half or two miles away.

.1* 1*5*0 Enter the town of Westf ield, Illinois.

.1* 1*5.1* An excellent view of the Illinoian till plain to the southeast.

STOP. Turn left (north). Enter the main north- south street of
Westf ield with caution.

.3 1*5*7 CAUTION. Turn right on main east-west street in village of
Westf ield.

.5 1*6.2 CAUTION. STOP. Turn left continue entering Route 1*9.

• 5 1*6.8 The sub- glacial channel that developed during the last advance

of the Shelbyville drained through the middle and first lobes
of the Shelbyville Moraine.

- 10 -

1.0 U7.8 Through this small stream drained a portion of the meltwaters

which accumulated behind the second lobe of the Shelbyville.
Ahead is the last and highest ridge of the Shelbyville.

•3 I48.I We have begun to climb the ridge of the Shelbyville.

.2 1*8.3 An excellent view to the north slope of the moraine and to

the east of the south side or front of the Shelbyville Moraine.

oil I18.7 Another view of the drainage way for the water which

accumulated behind the Shelbyville Moraine. The stream on the
right is still the drainage outlet for waters which now
accumulate • behind the inner Shelbyville Moraine.

1.9 50.6 We are on the crest of the moraine and are going down the back
slope of the inner Shelbyville.

.9 $1 •£ CAUTION r Slow. STOP. Turn left, entering Route 16.

To the left you will see the rolling character of the back
slope of the Shelbyville Moraine.

1«U 52.9 Note the sand in the roadcut on the left.

• 7 53.6 Slow. Enter the town of Ashmore.

IcO 5u«6 Another sand knoll.

2.1 56«7 A series of sandy ridges on the left. Most cf the streams

along this route are southward flowing entering Polecat Creek,
which developed on the back slope of the inner Shelbyville
Moraine,

1.5 58o 2 Slow. Turn right. Cross railroad with EXTREME CAUTION.

.5 58,7 Turn left (west).

.1 58.8 Slow. Turn left, entering pit of the Olen Humphre Stone
Company.

•3 59.1 This operation includes stripping the overburden from the gravel
and loading the gravel out, then taking the stone for crushing
opsratior;s. Follow the roadway to the right, aot into the
quarry but into an abandoned portion of the pit whers you will
see, beginning at the top cf the hill, till <n which a normal
soil profile xs developed, then a gravel zone sjme 10 feet
thick, then l'j feet of till. This till is 15 feet thj.ck, light
gray and almost completely unaltered. Then thsre &:© 10 to 20
feet of cross-bedded^ medium- to coarse-grained gravel containing
many mud balls. Lying beneath this and depending upon whether
or not the underlying limestone is even or uneven, a gray shale
of several feet in thickness may, or may not, be present,

- 11 -

You then will see the limestone, light gray in color and
ranging from 6 to 11 feet in thickness, followed by 2 feet
of shale, then 2 to 3 feet of very fossil if erous gray earthy
limestone, followed by k to 8 feet of medium gray earthy-
colored lime. Beneath this some 3 or h feet is a coal about
12 inches in thickness, which is followed by an underclay.
Immediately beneath the limestone is a black shale which
comes between the limestone and the coal.

Pennsylvanian sediments are unlike older sediments in that
they consist of many different and highly variable rock types,
the outstanding type being coal, which occurs in cycles. An
ideally complete cycle with its various units is shown near the
back of the itinerary. This type of rhythmic succession of
different kinds of strata is repeated in much the same sequence
some 50 times where the Pennsylvanian rocks are thickest. Each
rhythmic succession is called a cyclothem. The Millersville
limestone belongs in the Millersville Cyclothem and corresponds
to unit 9 in the ideally complete cyclothem at the back of the
itinerary.

The many different rock types in the Pennsylvanian system
indicate many rapid changes of environment which took place
repeatedly. At that time rivers were bringing sediments from
the north and east, possibly as far away as the present
Atlantic coast and the region south of Hudson Bay. The Midwest
was a low flat swampy area lying just a little above sea level,
but subject to frequent marine invasions as the land ros3 or
sank, or the sea level raised or lowered. That these conditions
existed is evident from the nature of the sediments. Mary of
the shales, limestones, and ironstones above the coals contain
marine fossils. The coals are believed to have formed in
broad fresh-water marshes somewhat like the Dismal Swamp of
Virginiae Most of the sandstones, conglomerates, underclays,
underclay limestones, and some shales probably accumulated in
fresh-water environments such as river valleys, lagoons, lakes,
or lowland plains. There is no area in the world today that has
conditions like those that existed during "Coal Measures" time.

The plants and trees that grew in "Coal Measures" time were
very luxuriant. In the jungle- like growths the plants most
common were huge tree ferns that had fronds five or six feet
long and grew to a height of more than $0 feet. Along with
them were seed ferns, now extinct, giant scouring rushes, and
large scale trees, which grew to heights of 100 feet or more.

The large scale trees we find preserved in the coals do not
have growth rings. The luxuriant growth and lack of growth rings
probably indicate that the climate that prevailed at this time
was warm and without seasonal change. As the plants fell into
the swampy waters they were partially preserved, buried by later
sediments and converted into coal.

V1

:>» r

It.

- 12 -

,8 $9*9 Cross the ditch with caution in leaving the quarry. The

early stage of the Shelbyville is believed to have brought
in the first 10 to 20 feet of gravel. The middle stage of
the Shelbyville brought in the drift which overrides and
incorporates, in part, some of the gravel in the till with
long fingers of gravel reaching 3^- to k feet up into the
unaltered till. Following this was another stage of gravel
which could have been brought in during the early development
of the inner stage of the Shelbyville Moraine. And this
gravel, in turn, was overridden by the inner moraine of the
Shelbyville.

We recommend for best fossil collecting the upper 2 feet of
the lower bench of the lime. However, much of the waste
material that has been brought out and dumped on the pile below
the abandoned portion of the pit comes from this zone, so good
hunting!

PART IV. GEOLOGICAL COLUMN - Greenup Area.

ERAS

PERIODS

EPOCHS

REMARKS

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CD
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Quaternary

Pleistocene

Exposed in Area:
Recent post-glacial stage
Wisconsin glacial stage
Illinoian glacial stage

a

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Tertiary

Pliocene

Miocene

Oligocene

Eocene

Paleocene

Wot present in area.

o

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•a

•a

•rt

(Age of rep-
tiles)

Cretaceous

Not present in area.

o

N
O

W
0)

Jurassic

Not present in Illinois.

£

Triassic

Not present in Illinois.

rtAncient Life"

Age of Amphibians
and Early Plants

Permian

Not present in Illinois.

McLeansboro

Livingston limestone, etc.
exposed.

Carbondale

In deep wells only.

Tradewater

Caseyville

In deep wells only.

o

•tH

o

o

Mississippian

Chester
Iowa

Thin sandstones, limer
stones and shales in
deep wells.

Limestone, sandstone and
shale in deep wells.

0)

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en to

<0j »H

Devonian

Dark shales and lime-
stones in deep wells.

Age of
Invertebrates I

Silurian

Magnesian limestones in
deep wells.

Ordovician

Maquoketa Shale, Middle
Ordovician Limestones,
and St. Peter Sandstone
& Shakopee limestone in
deetj wslls.

Cambrian

No data available.

Protero
Archeoz

zoic
oic

Referred to as "Pre
time

-Cambrian"

No data available.

7T"

UNGLACIATED \
AREA i^

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ILLINOIAN
DRIFT [~

PEORlAj

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h... \ MORAINES

I 1 KANKAKEE TORRENT

t==' AREAS

gwg LAKE CHICAGO
D22J AND OUTLET

f MARGIN OF
' WISCONSIN

SCALE

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SPRINGFIELD®

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ILLINOIS STATE GEOLOGICAL SURVEY H

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I

GLACIAL GEOLOGY OF NORTHEASTERN ILLINOIS

George E. Ekblaw

Revised 1957

10

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.v.\\:.\v. •'.•'.•

Shale, gray, sandy at top ; contains marine fossils and ironstone
concretions especially in lower part.

Limestone ; contains marine fossils.

Shale, black, hard, laminated ; contains large spheroidal concre-
tions ("Niggerheads") and marine fossils.
Limestone; contains marine fossils.

Shale, gray ; pyritic nodules and ironstone concretions common at
base ; plant fossils locally common at base ; marine fossils rare.

Coal ; locally contains clay or shale partings.

Underclay, mostly medium to light gray except dark gray at top ;
upper part noncalcareous, lower part calcareous.

Limestone, argillaceous; occurs in nodules or discontinuous beds;
usually nonfossiliferous.

rrr Shale, gray, sandy.

Sandstone, fine-grained, micaceous, and siltstone, argillaceous;
variable from massive to thin-bedded; usually with an uneven
lower surface.

AN IDEALLY COMPLETE CYCLOTHEM

(Reprinted from Fig. 42, Bulletin No. 66, Geology and Mineral Resources of the Marseilles,
Ottawa, and Streator Quadrangles, by H. B. Willman and J. Norman Payne)

(95 932-5M-4-5 9) -o^^n

Plate

Common Types of Illinois fossils

Cup coral

GRAPTOLITE

Lithostrotion
CORALS

Honeycomb coral

Archimedes

Fenestella

Branching

BRYOZOA

CRINOID PENTREMITE

Lingula Orbiculoidea

Productoid

Pentameroid

BRACHIOPODS

Plate 2

Common Types of Illinois fossils

"Clam"

"Scallop"
PELECYPODS

Coiled cone
(Nautilus)

Straight cone

CEPHALOPODS

Low - spired

High- spired

Flat - spired
GASTROPODS

Bumastus

Calymene
(coiled )

OSTRACODS
(greatly enlarged)

Calymene
(flat)

TRILOBITES