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557 IL6gu
no. 25

Survey

Waulsortian Mounds and Reservoir Potential

of the Ullin Limestone ("Warsaw") in Southern Illinois

and Adjacent Areas in Kentucky

Zakaria Lasemi, Janis D. Treworgy, Rodney D. Norby,
John P. Grube, and Bryan G. Huff

Geologic Field Trip, April 19, 1994

Sponsored by the Illinois Geological Society
and the Illinois State Geological Survey
Illinois Department of Energy and Natural Resources
ILLINOIS STATE GEOLOGICAL SURVEY

Digitized by the Internet Archive

in 2012 with funding from

University of Illinois Urbana-Champaign

http://archive.org/details/waulsortianmound25lase

Waulsortian Mounds and Reservoir Potential

of the Ullin Limestone ("Warsaw") in Southern Illinois

and Adjacent Areas in Kentucky

Zakaria Lasemi, Janis D. Treworgy, Rodney D. Norby,
John P. Grube, and Bryan G. Huff

Contributors

Garland R. Dever, Jr.

Kentucky Geological Survey
Terry Teitloff

Vulcan Materials Company, Kentucky
Richard D. Harvey

Illinois State Geological Survey

Guidebook 25

Geologic Field Trip, April 19, 1994

Sponsored by the Illinois Geological Society
and the Illinois State Geological Survey

Illinois Department of Energy and Natural Resources
ILLINOIS STATE GEOLOGICAL SURVEY

Morris W. Leighton, Chief

Natural Resources Building

615 East Peabody Drive

Champaign, Illinois 61820-6964

Phone 217/333-4747

Fax 217/333-2830

Printed by authority of the State of Illinois / 1994 / 1000
printed on recycled paper using soybean ink

CONTENTS

ULLIN LIMESTONE ("WARSAW") AND FORT PAYNE FORMATION:

OVERVIEW AND STOP DESCRIPTIONS

Zakaria Lasemi, Janis D. Treworgy, Rodney D. Norby,

John P. Grube, and Bryan G. Huff 1

OVERVIEW 1

Carbonate Rock Classification 5

Depositional Model 5

Hydrocarbon Potential 6

Overview of Stops 8

1 . Reed quarry 8

2. Ullin quarry 8

3. Jonesboro quarry 8

STOP DESCRIPTIONS 10

1. Reed quarry 10
Submound facies (Fort Payne) 10
Mound core facies (lower Ullin) 10
Mound flank and intermound facies (lower Ullin) 1 5
Sandwave facies (upper Ullin) 16

2. Ullin quarry 17
Lower Ullin 17
Upper Ullin 21

3. Jonesboro quarry 23

ACKNOWLEDGMENTS 25

REFERENCES 25

STRATIGRAPHIC AND BIOSTRATIGRAPHIC FRAMEWORK OF THE
ULLIN LIMESTONE ("WARSAW") AND FORT PAYNE FORMATION

Rodney D. Norby 26

STRATIGRAPHIC NOMENCLATURE 26

Ullin Limestone 26

"Warsaw," Warsaw Shale, and Warsaw Limestone 28

Fort Payne Formation 28

BIOSTRATIGRAPHY 29

Age of Springville Shale (Illinois), Basal Borden Group

(Indiana), and New Providence Shale (Kentucky) 29

Age of the Borden Siltstone (Illinois) and Main Part of the

Borden Group/ Formation (Indiana/Kentucky) 29

Age of the Fort Payne Formation 30

Age of the Ullin Limestone ("Warsaw") 30

REFERENCES 31

WAULSORTIAN MOUND, BRYOZOAN BUILDUP, AND
STORM-GENERATED SANDWAVE FACIES IN THE ULLIN
LIMESTONE ("WARSAW")

Zakaria Lasemi 33

OVERVIEW OF WAULSORTIAN MOUNDS 33

Facies 33

Source of Micrite 34

Distribution of Mounds 34

Hydrocarbon Production from Waulsortian Mounds 36

ULLIN ("WARSAW") AND FORT PAYNE FORMATIONS 36

Previous Studies 36

Depositional Environment 39

Waulsortian-type mounds of the lower Ullin 44

Lenticular grainstone piles of the lower Ullin 46

Sandwave facies of the upper Ullin 46

RESERVOIR POTENTIAL OF THE ULLIN LIMESTONE ("WARSAW") 46

REFERENCES AND SELECTED READINGS 48

PETROLEUM OCCURRENCE IN THE ULLIN LIMESTONE ("WARSAW")

John P. Grube 52

REFERENCES 55

VULCAN MATERIALS COMPANY REED QUARRY, LIVINGSTON
COUNTY, KENTUCKY

Garland R. Dever, Jr. and Terry Teitloff 56

REFERENCE 57

INDUSTRIAL USES OF THE ULLIN LIMESTONE ("WARSAW")

Richard D. Harvey 58

REFERENCES 59

APPENDIX

Production history to January 1 994 for Ullin ("Warsaw") fields 60

FIGURES

1 Generalized stratigraphic column (St. Peter and younger) for
southern Illinois 2

2 Regional map showing location of quarries, cores, other wells,

and cross sections 3

3 Wireline log showing various facies of the Ullin ("Warsaw") 4

4 Ullin ("Warsaw") and Fort Payne depositional model based

mainly on quarry exposures 7

5 Location of the Vulcan Materials Company Reed quarry 9

6 Diagram of the west wall in Reed quarry showing the bedded
submound facies (Fort Payne), mounds with flanking and inter-
mound facies (Ullin ["Warsaw"]), and the overlying sandwave

facies (upper Ullin) 11

7 Mound complex on the west wall of Reed quarry 1 1

8 Well bedded carbonates of the Fort Payne Formation

(submound facies) in Reed quarry 1 2

9 Thin section photomicrograph (plane light) of the Fort
Payne lime mudstone (submound facies) containing some
comminuted crinoids and scattered calcified sponge spicules
(needle-shaped grains) 12

1 0 Thin section photomicrograph (plane light) of the Fort Payne
Formation from a core, White County, Illinois 13

1 1 Close view of part of the mound core facies with well bedded,
dipping flank beds on the west wall of Reed quarry 13

1 2 Polished slab of the lime mudstone to wackestone facies of

the mound core in Reed quarry 14

13 Thin section photomicrograph (plane light) of the mound core
facies (Reed quarry) showing fenestrate bryozoan fronds,
scattered crinoid fragments, and rare ostracods 14

1 4 Chert bands and nodules in the mound core facies of the Ullin
("Warsaw") in Reed quarry 1 5

15 Thin section photomicrograph (plane light) of crinoid-bryozoan
wackestone to packstone facies of the flanking beds of the Ullin
("Warsaw") mound in Reed quarry 15

1 6 Polished slab of crinoid-bryozoan packstone from the flanking

bed of a mound in Reed quarry 16

1 7 Sandwave and intersandwave facies of the upper Ullin ("Warsaw")

in Reed quarry 16

1 8 Location of the Columbia Quarry Company's Ullin quarry 1 8

1 9 Interpretive sketch of a transported mound-like skeletal sand
pile with flanking bryozoan bafflestone buildup and overlying
sandwave facies 1 9

20 Photograph mosaic of a mound-like skeletal sand pile complex
with flanking bryozoan bafflestone beds exposed on the southeast

wall of Ullin quarry 19

21 Thin section photomicrograph of bryozoan-crinoid grainstone of

a mound-like skeletal sand pile 20

22a Flanking fenestrate bryozoan buildup from Ullin quarry 20

22b Reflected light photomicrographs of porous bryozoan

bafflestone buildup with coarse, relatively well preserved

fenestrate bryozoans characteristic of the reservoir

facies of the Ullin ("Warsaw") 21

23 Thin section photomicrograph of the porous bryozoan

bafflestone facies with rare crinoids 21

24 Location of the Columbia Quarry Company's Jonesboro

quarry, Union County, Illinois 22

25 Thin section photomicrograph (plane light) of fenestrate
bryozoan -rich, fine grained grainstone facies of the graded
storm bed in the upper Ullin Limestone ("Warsaw") in
Jonesboro quarry 23

26 Thin section photomicrograph (plane light) of crinoid-rich,
coarse grained facies of the graded storm bed in the upper Ullin
Limestone ("Warsaw") in Jonesboro quarry 23

27 Hummocky cross stratification, common in the upper Ullin
("Warsaw") in Jonesboro quarry 24

28 Laminated and graded-bedded bryozoan-crinoid grainstone
with escape burrow structure from the upper Ullin ("Warsaw")

in Jonesboro quarry 24

29 Stratigraphic terminology used in Illinois, Indiana, and

Kentucky for units in field trip region 26

30 Stratigraphic nomenclature and time correlation of units in

the field trip region 27

31 Facies distribution and depth zonation of Waulsortian mounds 35

32 South-north cross section (B-B') from Moultrie Country to

De Witt County, Illinois 37

33 Thickness of early Valmeyeran deltaic sediment 38

34 South-north cross section (A-A') from Wayne County to

Effingham County, Illinois 40

35 Thickness of the Ullin Limestone ("Warsaw") 42

36 Thickness of the Fort Payne Formation 43

37 Thin section photomicrograph of the lime mudstone core
facies of a Waulsortian-type mound in the Ullin ("Warsaw")

from a core taken about 12 miles east of Ullin quarry, Illinois 45

38 Thin section photomicrograph of the wackestone core facies

of a Waulsortian-type mound 45

39 Thin section photomicrograph of a core sample from White

County, Illinois 47

40 Distribution of Ullin/Harrodsburg/"Warsaw" hydrocarbon

production in the Illinois Basin 53

41 Porosity log of the Porter-Weaver Community no. 1 , one of the

better Ullin ("Warsaw") producers in Johnsonville Consolidated 54

TABLE

1 Classification of limestones according to depositional texture 5

APPENDIX

Production history to January 1994 for Ullin ("Warsaw") fields 60

ULLIN LIMESTONE ("WARSAW")

AND FORT PAYNE FORMATION:

OVERVIEW AND STOP DESCRIPTIONS

Zakaria Lasemi, Janis D. Treworgy, Rodney D. Norby,
John P. Grube, and Bryan G. Huff

OVERVIEW

The Ullin Limestone ("Warsaw") and Fort Payne Formation (fig. 1) will be
examined in three quarries in southernmost Illinois and western Kentucky
(fig. 2). The petroleum industry in southern Illinois has referred to the lime-
stone unit that underlies the Salem Limestone as the "Warsaw"; however, it
differs lithologically from the type Warsaw Shale of western Illinois. Lineback
(1966) renamed the "Warsaw" of southern Illinois the Ullin Limestone and
restricted the term Warsaw \o the calcareous shale of western Illinois. We
follow Lineback's terminology in this guidebook (see Norby, this guidebook).

A wireline log from Wayne County, Illinois (fig. 3), shows one type of log
response for the Ullin and Fort Payne in the subsurface; the porous and
nonporous zones are clearly differentiated. Distinguishing individual fades,
however, requires a study of samples or cores. The number and thickness
of porous and nonporous zones vary significantly from one area to another.
This field trip provides an opportunity to examine lithologic and sedimen-
tologic relationships that exist between various facies within the Ullin and
Fort Payne and are not easily recognizable on the basis of logs, cuttings,
and cores.

One of the main hypotheses of our ongoing research has been the possible
presence of Waulsortian-type carbonate mounds within the Ullin Limestone.
Recognition of mounds in the Ullin in outcrop supports this hypothesis. Waul-
sortian mounds (named after the town of Waulsort in Belgium) are early to
mid-Mississippian (late Tournaisian through early Visean) carbonate bodies
with a lime mudstone-wackestone core facies flanked by dipping crinoid-
bryozoan packstone-grainstone beds. These mounds are morphologically
similar to reef mounds such as those in the Silurian carbonates of the Illi-
nois Basin, except for the lack of fossil remains from frame-building
organisms such as corals and stromatoporoids. Waulsortian mound
facies are prolific hydrocarbon producers in several regions of North
America (MacQuown and Perkins 1982, Ahr and Ross 1982, Davies, et al.
1989, Burke and Diehl 1993). Recent discoveries of hydrocarbons in the
Ullin Limestone ("Warsaw"), in part associated with the Waulsortian mound
facies, indicate that the Ullin has a greater reservoir potential than previously
recognized. During this field trip, we will observe some reservoir as well
as nonreservoir facies of the Ullin Limestone.

Figure 1 Generalized stratigraphic column (St. Peter and younger) for southern Illinois. Study inter-
val is highlighted. Formations or members that contain hydrocarbon pay zones are shown in bold
type. Abbreviations: Alexandrian (Alex.), Cayugan (Cayu.), Upper Devonian (Up.), Kinderhookian
(K.), Valmeyeran (Val.), and Virgilian (Virg.). Variable vertical scale. (Modified from Howard 1991.)

30 60 mi

Figure 2 Regional map showing location of quarries, cores, other wells, and cross sections.

DAVIS

Dulaney no. 1

T3S-R5E-Sec 6 NE/C SW 1/4

Wayne Co., IL

Salem

Ullin
("Warsaw")

Fort Payne

Springville

Chouteau

New Albany

7
1

3900

4000

4100

4200

4300

4400

4500

4600

4700

feet

brown to brownish gray, argillaceous, slightly
cherty lime mudstone to wackestone

very light gray crinoid-bryozoan packstone to
grainstone, in part oolitic

BRYOZOAN PATCH REEF
very light gray vuggy bryozoan baff lestone
buildup

SANDWAVE FACIES
light gray interbedded lime mudstone and crinoid-
bryozoan grainstone

FLANKING BRYOZOAN BUILDUP
light gray to white, vuggy bryozoan bafflestone
overlain by crinoidal wackestone to packstone
(intermound)

MOUND CORE FACIES
slightly cherty, light gray lime mudstone to
wackestone

FLANKING TO INTERMOUND FACIES
light gray crinoidal grainstone

MOUND CORE FACIES
slightly cherty, brownish gray lime mudstone to
wackestone

SUBMOUND FACIES
dark brown, very argillaceous, in part cherty lime
mudstone

shale

lime mudstone

black shale

Gamma

Resistivity

Figure 3 Wireline log (Davis
Dulaney no. 1, Wayne County,
Illinois) showing various fades of
the Ullin ("Warsaw") including the
inferred mound facies and in situ
bryozoan bafflestone buildup as
seen in drill cuttings. The term
bryozoan patch reef is used for
the more isolated and smaller
bryozoan bafflestone buildups
in the upper Ullin. Petrographi-
cally, these bryozoan patch reefs
are similar to bryozoan bafflestone
buildups associated with Waulsor-
tian mounds in the lower part of
the Ullin.

Table 1 Classification of limestones according to depositional texture (modified from Embry and
Klovan 1971, and Dunham 1962).

allochthonous limestones
(original components not organically bound during deposition)

autochthonous limestones

(original components organically

bound during deposition)

<10% components (>2 mm)

>10% components
(>2 mm)

I »

(A (|)

O (ft

>. «

$ *

a 3

3
(0

.2 2

i_ TO
O *-

>> 3

= 1

supported by organisms
which build a rigid framework

contains lime mud
(<.03 mm)

no lime
mud

•o

9
C

o
a.

3
(0
i

•a
(0

■o
o

o
a
a.

3
(A
i

C
0
C

E
o
u

mud-supported

grain-supported

<10% grains

(>.03 mm,

<2mm)

>10%
grains

mudstone

wackestone

packstone

grainstone

floatstone

rudstone

bafflestone

bindstone

framestone

Carbonate Rock Classification

Terminology for carbonate rocks used in this guidebook (table 1 ) follows that
proposed by Embry and Klovan (1971), who expanded on Dunham's (1962)
carbonate classification. This classification is based on matrix-particle relation-
ships, particle size, and the distinction between particles that are organically
bound (autochthonous) or not organically bound (allochthonous).

Bafflestone is generally defined as a limestone containing in situ stalked-shaped
fossils, which may trap sediments by acting as baffles (Embry and Klovan 1 971 ).
In this guidebook, the term bafflestone refers to in situ bryozoan-dominated
buildups that developed on the flank and crest of Waulsortian-type mounds
or on transported skeletal sand piles. The term bryozoan patch reef is used for
the smaller and more isolated bryozoan-dominated bafflestone buildups in
the upper Ullin. The term coated grains refers to allochems with dark micritic coats
possibly of algal origin; micritized grains result from microboring of allochems
and later infilling of those microborings by micritic sediments or cements.

Depositional Model

The Ullin Limestone of the Illinois Basin contains (1 ) Waulsortian-type carbonate
mound complexes, (2) transported mound-like to lenticular bryozoan-crinoid
sand piles (packstones to grainstones), and (3) storm -gene rated sandwaves.

Waulsortian-type mounds developed below storm-wave base in a deeper
water, outer ramp setting and, rarely, in shallower, mid-ramp environments
(for ramp terminology, see Burchette and Wright 1992). Mound develop-
ment was terminated as gradual shallowing up to storm-wave base occurred
through time. Subsequently, storm-generated sandwaves, lenticular to mound-
like skeletal sand piles, and bryozoan patch reefs became widespread in a
mid-ramp setting during this later stage of the Ullin deposition. Lenticular
sand piles are moderately sorted and partially laminated, suggesting deposi-
tion by currents rather than in situ development. The fine grained size and
mound-like geometry suggest that the lenticular sand piles were deposited in
more distal parts of the mid-ramp setting than were the overlying storm-
generated sandwaves. Facies of Waulsortian-type mounds and lenticular

skeletal sand piles generally coalesce laterally and vertically into com-
plex carbonate bodies that range from 50 to 500 feet long and 20 to 70 feet
thick in outcrop, and thicken basinward in the subsurface of Illinois.

A schematic diagram (fig. 4), based mainly on quarry exposures, illustrates
our model for development of mounds and related facies within the Ullin
(see Lasemi, this guidebook). The typical log character for some of these
facies in the subsurface is illustrated in a sample wireline log from Wayne
County (fig. 3). In the early stage of Ullin deposition (fig. 4a), Waulsortian-
type mounds (mudstone to wackestone) were developed in the outer ramp
setting. In the deeper part of the outer ramp (Reed quarry), mounds grade
into the dark-colored, argillaceous, spiculitic lime mudstone of the Fort Payne
Formation. These mounds are flanked by dipping, well bedded, transported,
low-porosity wackestone to packstone. In the shallower part of the outer ramp
setting (ISGS Miller nos. 1 and 2 cores), an in situ bryozoan-crinoid bafflestone
buildup developed on the crest and flank of the mound core. This bafflestone
buildup is generally porous and could be a potential hydrocarbon reservoir
where permeable. Bryozoan-crinoid sand accumulated as storm-generated
sandwaves and lenticular sand piles in the mid-ramp setting (Ullin and
Jonesboro quarries) and as a debris apron in intermound areas of the outer
ramp setting. This facies becomes muddier basinward.

By the late stage of Ullin deposition (fig. 4b), the lower part of the Ullin had
built up to a shallower environment above storm wave base. This late stage
represents a progradational phase of Ullin deposition. Storm-generated
sandwaves (grainstone) are widespread in the upper part of the Ullin. Log
character and sample studies indicate that this is generally a porous facies.
The sandwaves grade from thicker and coalesced units (up to 1 50 feet thick)
in shallower, mid-ramp settings (Jonesboro quarry) to more isolated units
basinward (Reed quarry). The isolated sandwaves interfinger with the denser
intersandwave facies, which becomes muddier basinward. Porous bryozoan-
dominated bafflestone buildups are also present in the upper Ullin. These
buildups developed as patch reefs on isolated mud mounds and mound-like
skeletal sand piles. Examination of drill cuttings and core from some producing
wells indicates that the hydrocarbon reservoir is mainly in these bryozoan
patch reefs in the upper Ullin.

Both sandwaves and isolated mounds probably formed depositional highs in
the upper part of the Ullin (fig. 4b). Cluff (1984) also identified the Ullin-Salem
contact as irregular. The highs may have been sites for development of oolitic
shoals during deposition of the upper Ullin and/or lower Salem Limestones.
Thus, the oolite shoals in the Salem may provide a means of locating isolated
mounds and sandwaves in the Ullin, all potential hydrocarbon reservoirs.

Hydrocarbon Potential

Waulsortian-type mound facies similar to those in the Ullin Limestone are
prolific hydrocarbon reservoirs in several regions in North America. In the
Illinois Basin the Ullin is an oil-producer (see appendix), but its potential as
a reservoir has been largely overlooked. Recent drilling in southern Illinois
has encountered prolific petroleum-producing zones within the Ullin Limestone.
This information along with large cumulative production rates from several older

Jonesboro quarry

EARLY STAGE OF ULLIN ("WARSAW ') DEPOSITION

No. 1 and No. 2
Ullin quarry , , Miller cores

Reed quarry

mid-ramp

outer ramp.

basin

LATE STAGE OF ULLIN ('WARSAW") DEPOSITION

A*A

cherty

storm-generated skeletal (crinoid-bryozoan)
sandwave (G)

intersandwave facies

transported skeletal sand facies in intermound
areas and on mound flanks

WZA

1=1

outer ramp ■

bryozoan-crinoid baff lestone buildup facies
(potential hydrocarbon reservoir)

transported skeletal sand facies forming dense
leticular mound-like deposits in shallower areas

mudstone-wackestone core facies of Waulsortian-
type mounds

Fort Payne

basin

Figure 4 Ullin ("Warsaw") and Fort Payne depositional model, based mainly on quarry exposures: (A) early stage
of the Ullin mound development on a ramp after the transgression of the Fort Payne sea (see fig. 31 for description of Waulsor-
tian facies B and C); (B) late stage of the Ullin deposition representing a shallow ramp with widespread sandwave and bryozoan
patch reef facies developed on a skeletal grainstone or lime mudstone high. Horizontal distance is approximately 70 miles;
vertical scale is approximately 300 feet (outcrop) to 700 feet (subsurface). Slope of ramp is exaggerated. Ramp subdi-
visions based on Burchette and Wright 1992. Symbols used on diagram: M = mudstone, W = wackestone, P = packstone,
G = grainstone.

wellsinthe Illinois Basin indicates that the Ullin has a greater reservoir
potential than previously recognized.

Because of excellent preservation of intra- and interparticle porosity, the
bryozoan bafflestone buildup has a high potential for reservoir development
where permeable. High porosity is also characteristic of debris aprons (depos-
ited downslope from the mound in intermound areas) and storm-generated
sandwaves in the Ullin. Porosity, permeability, and reservoir quality may be
variable, however, and depend on the relative abundance of crinoid fragments.
This is partly because crinoids are susceptible to overgrowth cementation, which
can occlude porosity. Furthermore, permeability could be reduced by the
presence of micrite, especially in bryozoan bafflestone buildups. In such
cases, the reservoir permeability may be enhanced by fracturing (Tom Partin,
consultant, personal communication 1994).

Overview of Stops

Facies observed in the quarries represent a transition from what has been
interpreted by the authors as a relatively deep-water setting (Reed quarry in
Kentucky) to a relatively shallower water setting (Ullin and Jonesboro quar-
ries in Illinois). Detailed descriptions of quarry exposures begin on page 10.

The various facies will be discussed at each of the stops. Between stops 1 and
2, we will stop at the Kentucky Dam visitors area to have lunch while watch-
ing the river traffic.

1. Reed quarry, about 30 miles east of Metropolis, Illinois, in
Kentucky The Fort Payne, the various facies of the overlying
Waulsortian mound complexes of the lower part of the Ullin, and
the sandwave and intersandwave facies of the upper part of the Ullin
are well exposed here. The morphology of the mounds is clearly
observable. The only exposed facies in this quarry that is a potential
hydrocarbon reservoir is the transported facies in the upper part of
the Ullin.

2. Ullin quarry about 1 mile north of Ullin, Illinois Numerous
small lenticular mounds can be seen in the lower 45 to 50 feet of the
quarry. In one area, a mound complex of the lower part of the Ullin is
flanked by a thin reservoir-quality, bryozoan bafflestone facies.

3. Jonesboro quarry, about 6 miles south of Jonesboro, Illinois

The crossbedded packstone-grainstone of the upper part of the
Ullin is well exposed in this quarry. There is evidence for storm
deposition of this interval. The relatively high porosity of this facies
(see Harvey, this guidebook) makes it promising as a potential hydro-
carbon reservoir where permeable.

Figure 5 Location of the Vulcan Materials Company Reed quarry, 20-G-15, 16-G-16; Calvert City
and Grand Rivers 7.5-minute quadrangles.

STOP DESCRIPTIONS

Stopl. Reed quarry

B20-G-15, 16-G-16; Calvert City and Grand Rivers 7.5-minute quadrangles,
Livingston County, Kentucky (fig. 5; see Dever and Teitloff, this guidebook)

The bedded submound facies (Fort Payne), the mound core facies (lower Ullin),
the mound flank and intermound facies (lower Ullin), and the overlying sandwave
and intersandwave facies (upper Ullin) will be examined in this quarry (figs. 4,
6, 7). The Ullin of Illinois is roughly equivalent to the Warsaw and upper Fort
Payne of Kentucky (see Norby, this guidebook). Although the Salem Limestone
is partly exposed in this quarry, it will not be covered in this guidebook.

The carbonate rocks exposed in this quarry include approximately the upper
1 50 feet of the Fort Payne Formation, approximately 240 feet of the Ullin Lime-
stone, and the lower part of the Salem Limestone. Total thickness of the Fort
Payne is approximately 500 to 600 feet in this area (Dever and McGrain 1 969).

Submound facies (Fort Payne) This facies (fig. 8) is a well bedded, gener-
ally 0.5 to 2 feet thick, argillaceous, in part pyritic, spiculitic, and siliceous
limestone (fig. 9) with scattered chert bands. It is typically dark brown to dark
gray brown and contains some transported crinoid and rare bryozoan fragments.
A similar lithology also characterizes the Fort Payne in the subsurface of Illinois
(see also Lineback and Guff 1985). The dark coloration is probably due to the
presence of organic matter in the rock, which emits a strong fetid odor when
it is broken or sawed. Further work is needed to assess the potential of the
Fort Payne as a hydrocarbon source rock.

Dark gray shale partings are common on bedding planes. Laminations are
commonly preserved within the Fort Payne because of the lack of biotur-
bation (fig. 10). Preliminary petrographic data reveal the presence of rare
pelagic radiolarians. These features and the presence of Chondrites and
Zoophycus trace fossils (fig. 10) indicate that the Fort Payne was deposited
under disaerobic conditions in a relatively deep-water setting, as suggested by
Lineback and Cluff (1985).

The Fort Payne Formation in part of this quarry contains large wedges of
well bedded lime mudstone. The wedge bases are in sharp contact with the
underlying unit. The origin of these features may be related to slumping during
or after deposition.

Mound core facies (lower Ullin) Overlying the bedded submound facies of
the Fort Payne is a series of carbonate mud mounds. A mound complex is
well exposed on the west wall of the quarry (figs. 6, 7, 11). This appears to
be a composite mound consisting of laterally overlapping individual mounds
and onlapping flanking beds that dip about 20°. The mound complex is about
60 to 70 feet thick and 500 feet wide. The core of the mound is dark gray, mas-
sive lime mudstone to wackestone (fig. 12) with common bryozoan fronds,
crinoids, and scattered calcified sponge spicules (fig. 13). The mound, in part,
appears to be composed of thick multiple layers, which may represent various
stages of mound growth during vertical accretion. The massive nature of the
mound core is in sharp contrast with the well bedded submound facies.

REED QUARRY-WEST WALL

sandwave
facies

mound-

intermound

facies

submound
facies
(Ft. Payne)

chert bands

storm-generated skeletal sandwave (G)

(G = potential hydrocarbon reservoir)

intersandwave (M-W) facies

\\ flanking and intermound areas

mudstone-wackestone core facies
of Waulsortian-type mounds

Fort Payne

Figure 6 Diagram of the west wall in Reed quarry showing the bedded submound facies (Fort Payne),
mounds with flanking and intermound facies (Ullin ["Warsaw"]), and the overlying sandwave facies (upper
Ullin). Symbols used on diagram: M = mudstone, W = wackestone, P = packstone, G = grainstone.

Figure 7 Mound complex on the west wall of Reed quarry (see figs. 6 and 11). C = mound-core
facies, F = flanking facies, I = intermound facies. Mound core (C) is approximately 70 feet high, top
indicated by white dashed line.

idfw

Figure 8 Well bedded carbonates of the Fort Payne Formation (submound fades) in
Reed quarry. Quarry wall is approximately 60 feet high.

Figure 9 Thin section photomicrograph (plane light) of the Fort Payne lime
mudstone (submound facies) containing some comminuted crinoids and
scattered calcified sponge spicules (needle-shaped grains). Reed quarry,
western Kentucky. Bar scale = 1 mm.

Figure 10 Thin section photomicrograph
(plane light) of the Fort Payne Formation
from a core. Note well preserved lamina-
tion, suggesting the lack of bioturbation.
Light colored, churned area on the left in
the central part of the photomicrograph
might be Zoophycus, a trace fossil. Core
sample from 4,182 foot depth, Superior
Oil no. C-17 Ford, NW SW SE Sec. 27,
T4S, R14W, White County, Illinois. Bar
scale = 0.5 cm.

Figure 11 Close view of part of the mound core facies (see figs. 6, 7) with well bedded,
dipping flank beds on the west wall of Reed quarry. Flanking beds become horizontally bedded
in intermound area to the right. C = core facies, F = flanking facies, I = intermound facies. Quarry
wall is approximately 70 feet high in center of photograph.

Figure 12 Polished slab of the lime mudstone to

wackestone facies of the mound core in Reed quarry

(see fig. 1 1 ). Note fenestrate bryozoan fronds and

scattered crinoid fragments (light colored).

Bar scale = 2 5 cm Figure 13 Thin section photomicrograph (plane light)

of the mound core facies (Reed quarry) showing
fenestrate bryozoan fronds, scattered crinoid frag-
ments, and rare ostracods (e.g., fingernail-shaped
grain at top left). Some of the small needle-shaped
grains may be sponge spicules. Bar scale = 0.5 cm.

The mound contains abundant narrow and elongate chert bands (fig. 14) that
range from less than 1 inch to a few inches thick and from a few inches to
several feet long. Crinoid and rare bryozoan debris form a geopetal fabric at
the base of some chert bands. This feature suggests to us that chert may
have formed as silica precipitated in preexisting cavities. Most cherts are very
dark gray to black and commonly pyritic, suggesting the presence of decom-
posing organic matter prior to or during chert formation. Closer examination
shows that the chert bands follow the orientation of the mound. Chert bands
rarely crosscut the mound flank into the bedded flanking facies. The chert,
whatever its origin, probably formed simultaneously with mound development.

Numerous other mounds are present throughout the quarry at about the same
level. Exposure of these mounds is poor, but their presence can be inferred
from the dipping flank beds. Some mounds (for example, on the north wall)
are bedded (2-3 feet thick), lenticular bodies up to 20 feet thick. Chert bands
are rare, but shale partings are relatively common on bedding planes.
Flanking beds are partially crinoid-rich and vary from wackestone to rare
occurrences of crinoidal packstone with fragmented bryozoan matrix.

Figure 14 Chert bands and nodules in the mound core facies of the Ullin
("Warsaw") in Reed quarry. Hammer (lower left) for scale.

Figure 15 Thin section photomicrograph (plane light) of crinoid-bryozoan
wackestone to packstone facies of the flanking beds of the Ullin ("Warsaw")
mound in Reed quarry. Note the calcite-filled microfracture. Bar scale = 1 mm.

Mound flank and intermound facies (lower Ullin) Flanking beds onlap
the mound core with a dip of about 20° (figs. 6, 7, 11). They are well bedded
lime mudstone and wackestone (fig. 15) with scattered crinoid and bryozoan
fragments. Crinoid concentrations can be quite high locally, resulting in thin
crinoidal packstone beds (fig. 16). Some chert bands are also present in the
flanking beds, which grade into horizontally bedded, cherty lime mudstone
facies in intermound areas (figs. 6, 7, 11). Graded bedding may be present

*, '' .*r*''',H* '**' vfc,V- '

'Figure 16 Polished slab
of crinoid (light colored)
and bryozoan (dark) pack-
stone from the flanking bed
of a mound in Reed quarry.
Note inclined lamination. Bar
scale = 2.5 cm.

Figure 17 Sandwave (light-colored, crinoid-bryozoan grainstone) and inter-
sandwave (dark, dense cherty lime mudstone) facies of the upper Ullin
("Warsaw") in Reed quarry, Kentucky. Quarry wall in center is approximately
70 feet high. Note person at lower right for scale.

in the intermound area, indicating redeposition by downslope off-mound
transport. Because of their mud-dominated nature, the flanking beds in this
quarry are poor candidates for reservoir development.

Sandwave facies (upper Ullin) Overlying the mound and flanking facies
are a series of wedge-shaped, skeletal sand bodies (figs. 6, 17) composed
mainly of crinoid-bryozoan packstone and grainstone. These skeletal sand
bodies appear to be mostly massive due to partially obscured surface expo-
sure or bioturbation, but some show large-scale, inclined laminations. The

geometry of these sand bodies indicates that they probably were deposited
as asymmetrical sandwaves. Large-scale inclined bedding may represent
slipface migration of the sandwaves. The sandwave facies grades laterally
into a dense, cherty lime mudstone of the intersandwave facies. Thin shale
partings occur in places, suggesting deposition from waning currents. The
sandwaves are interpreted to be storm deposits in relatively deep water,
below normal wave base. We will see clearer evidence for storm deposi-
tion at Stop 3 in the Jonesboro quarry.

Although the sandwave facies is well cemented at this outcrop, it is generally
porous in the subsurface. The dense intersandwave lime mudstone facies pro-
vides an excellent barrier for entrapment of hydrocarbons. The low porosity
of the sandwave facies in outcrop may be due to a higher susceptibility to
subaerial diagenesis and fresh-water cementation (work in progress). Preser-
vation of porosity in the sandwave facies in deeper parts of the basin may be
related to rapid burial that preceded subaerial exposure and thus prevented
fresh-water cementation. Furthermore, the presence of minor amounts of
marine cements in some areas may have been instrumental in preventing
the occlusion of pores during diagenesis that occurred after burial of the
deposits. Marine cement was apparently sufficient to stabilize the rock fabric
without totally occluding all primary pore spaces, which resisted compaction
and pressure solution during burial.

Stop 2. Ullin quarry

■ S1/2 SW NE and N1/2 NW SE Section 14, T14S, R1W; Dongola
7.5-minute quadrangle, Pulaski County, Illinois (fig. 18)

An exposure of about 180 feet of the Ullin Limestone appears, upon first
inspection, to consist of two facies. One facies, which forms the basal 45 to
50 feet of the quarry, includes a medium gray, in part slightly cherty packstone to
grainstone typical of the lower Ullin (fig. 4b). The upper facies is mainly a light
gray, fine grained, crinoid-bryozoan packstone to grainstone, typical of the
upper Ullin.

Lower Ullin Close examination of carbonates in this quarry reveals a complex
facies relationship. The lower Ullin appears to be composed of a series of len-
ticular carbonate bodies, which may coalesce laterally and vertically into more
complex carbonate mounds (fig. 4b). Topographic irregularities in the quarry
floor also imply the presence of mounds in the lower, unexposed Ullin. These
lenticular mounds, as exposed in the lowest level of the quarry, are about 20
to 30 feet thick and 50 to 200 feet long, and have a lower (<5°) flanking slope
angle than that observed in Reed quarry. As a result of blast fracturing, the
form of the mounds is not as apparent here as in Reed quarry.

The core of these lenticular mounds is characterized by a generally mas-
sive to thick bedded limestone; fine lamination may be present in places.
Thin section petrography reveals that the core facies is a moderately sorted, fine
grained, bryozoan-crinoid grainstone. Unlike that of the mound core facies in
Reed quarry, the micrite content is negligible, mainly limited to infilling of
bryozoan zooecia. The lamination, moderate sorting, and lack of micrite matrix
are evidence for deposition of these lenticular carbonate bodies by currents.

Figure 18 Location of the Columbia Quarry Company's Ullin quarry, S1/2 SW NE and N1/2 NW
SE Sec. 14, T14S, R1W; Dongola 7.5-minute quadrangle, Pulaski County, Illinois.

The core fades is slightly cherty with white-weathering, elongate chert nodules
(0.5-2 inches thick and a few inches to several feet long) that generally
occur parallel to bedding. Many of these cherts have dark gray mottlings and
speckles and may contain some disseminated pyrite and pyritic nodules.
Dark gray mottling and pyrite imply a possible relationship between decom-
position of former organic matter and genesis of the cherts. The massive
core facies grades laterally and vertically into slightly coarser, lighter gray,
well bedded and laminated to hummocky cross-laminated, crinoid-bryo-
zoan grainstone facies.

ULLIN QUARRY-SOUTHEAST WALL

storm-generated skeletal sandwave (G)
intersandwave (P-G) facies

bryozoan-crinoid bafflestone buildup facies
(potential hydrocarbon reservoir)

transported lenticular (mound-like) skeletal
sand pile (storm-generated?)

Figure 19 Interpretive sketch (see fig. 20) of a transported mound-like skeletal sand pile (bryozoan-
crinoid grainstone) with flanking bryozoan bafflestone buildup (potential reservoir facies) and overly-
ing sandwave facies (Ullin quarry, Illinois). Vertical scale approximately 50 feet; horizontal scale
approximately 150 feet. Symbols used on diagram: P = packstone, G = grainstone.

Figure 20 Photograph mosaic of a mound-like skeletal sand pile complex with flanking bryozoan bafflestone
beds (area between dashed lines) in the lower Ullin ("Warsaw") exposed on the southeast wall of Ullin quarry
(see fig. 19).

Slightly higher in the quarry on the southeast wall along the main ramp,
several lenticular mounds and mound complexes may be observed (figs. 19,
20). These mounds coalesce laterally and vertically, resulting in a complex
mound system overlain by coarser packstone to grainstone facies of the upper
Ullin. Similar to individual mounds, the core facies in these mounds is slightly
cherty, massive grainstone (fig. 21). The apparent width of the mound
complex is about 1 50 to 200 feet.

Figure 21 Thin section photo-
micrograph (plane light) of
bryozoan-crinoid grainstone

| of a mound-like skeletal sand
pile in Ullin quarry. White
areas are syntaxial calcite
cement overgrowths on crinoid

I fragments (gray).
w& Bar scale = 1 mm.

^Jj; '*;V 4& * x 4P

l^jt' m. * y » * ■■* «4i *•» ** '**

'4*n f-%,^1 I Figure 22a Flanking fenes-
I trate bryozoan buildup from

*i v i"^* « Ullin °iuarry (see fi9s- 19- 2°)-

^ r« ♦>- Bar scale = 0.5 cm.

The flanking facies consists of a highly porous and permeable bryozoan (90%)
bafflestone buildup. Although it is about 1 to 5 feet thick at the top of the mound,
it thins laterally and pinches out down the flank of the mound (figs. 1 9, 20).
This well bedded bafflestone facies has beds 1 to 2 inches thick and an
apparent dip of about 3° to 5° in the same direction as the mound flanks. It
consists of generally well preserved fenestrate bryozoans (fig. 22a).

This facies occurs in at least three horizons in this mound complex, separated
by the dense core facies (figs. 19, 20), forming vertically stacked mounds.
Similar facies are also present at various horizons within the Ullin in the sub-
surface (figs. 3, 22b). The high porosity and permeability of this bafflestone
facies (fig. 23) makes it an excellent candidate for reservoir development.

Figure 22b Reflected light
photomicrographs of porous
bryozoan bafflestone buildup
with coarse, relatively well
preserved fenestrate bryo-
zoans characteristic of the
reservoir facies of the Ullin
("Warsaw"). Core sample
(Milestone Petroleum,
Burlington-Northern no.1, SE
SENWSec. 14,T6S,R2E,
Franklin County, Illinois). Bar
scale = 0.5 cm.

Figure 23 Thin section photo-
micrograph (cross-polarized
light) of the porous bryozoan
bafflestone facies (figs. 19,
20) with rare crinoids (Ullin
quarry). Note high porosity
(black). Bar scale = 1 mm.

This facies appears to be thicker and more laterally extensive northward in
the subsurface. This facies of the Ullin produces hydrocarbons in Illinois.

Upper Ullin Very light gray, laminated to hummocky cross-laminated,
medium to coarse grained, bryozoan-crinoid packstone-grainstone is inter-
bedded with medium light gray, massive to slightly laminated, fine grained
packstone-grainstone. This facies (figs. 4b, 19) is interpreted to represent
interfingering sandwave and intersandwave facies (5-10 feet thick) similar
to those in Reed quarry. Instead of the lime mudstone intersandwave facies
that occurs in Reed quarry, a fine grained packstone-grainstone occurs here
in the Ullin quarry. The low carbonate mud content of this facies, compared
with that in the Reed quarry is most likely due to deposition in a somewhat

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311

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1A ) ^ft*

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Jonesboro
quarry

Quarry

ir\

. ..UNION.. CO
PULASKI CO

Figure 24 Location of the Columbia Quarry Company's Jonesboro quarry (NE SW Sec. 20,
T13S, R1W; Dongola 7.5-minute quadrangle, Union County, Illinois).

shallower setting and thus higher energy conditions. The very light gray, coarser
fades includes well developed, large-scale, inclined laminations possibly formed
as a result of slipface migration of the sandwaves as a result of storm-generated
currents. Storm deposition is supported by the presence of hummocky cross-
stratification, as commonly observed in the adjacent and overlying units.

Figure 25 Thin section
photomicrograph (plane
light) of fenestrate
bryozoan-rich, fine grained
grainstone facies of the
graded storm bed in the
upper Ullin Limestone
("Warsaw") in Jonesboro
quarry. Bar scale = 1 mm.

Figure 26 Thin section
photomicrograph (plane
light) of crinoid-rich, coarse
grained grainstone facies of
the graded storm bed in
the upper Ullin Limestone
("Warsaw") in Jonesboro
quarry. Note calcite cement
overgrowths (white) on cri-
noids. Dark fragments are
bryozoans. Bar scale = 1 mm.

Stop 3. Jonesboro quarry

■ NE SW Section 20, T13S, R1 W; Dongola 7.5-minute quadrangle, Union
County, Illinois (fig. 24)

The uppermost and possibly the shallowest facies of the Ullin to be seen on this
field trip is exposed in this quarry (fig. 4b). The entire quarry section consists
of about 1 50 feet of the upper Ullin. The limestone is dominated by a very light
gray, coarse to very coarse crinoid-bryozoan to bryozoan-crinoid grainstone. The
rock is well laminated and cross-laminated with alternating beds of very light gray,
fine grained bryozoan-rich hash (fig. 25) and darker crinoid-rich sand (fig. 26).
Graded bedding and hummocky cross-laminations (fig. 27) are very common
throughout the unit. Evidence of bioturbation is minimal in these rocks, but

escape burrow structures (fig. 28) were observed in some beds. These
features in the Ullin Limestone in this quarry indicate relatively rapid deposi-
tion, probably by storm currents. The uppermost part of the Ullin in this quarry
contains large-scale planar and trough crossbedding, indicating a more agitated
depositional environment (possibly within normal wave base) than that for the
rest of the Ullin.

Figure 27 Hummocky cross stratification, common in the upper Ullin ("Warsaw")
in Jonesboro quarry.

Figure 28 Laminated and graded-bedded bryozoan-crinoid grainstone with
escape burrow structure from the upper Ullin ("Warsaw") in Jonesboro quarry.

ACKNOWLEDGMENTS

The field trip leaders thank all the people who assisted with the preparations
for this trip. Some contributors to this guidebook also provided valuable serv-
ices: Garland Dever of the Kentucky Geological Survey provided geological
assistance at Reed quarry; Perry Donahoo, president of Reed Crushed Stone
Company, a division of Vulcan Materials Company, strongly supported our
geological research; Terry Teitloff, manager of Technical Services and Quality
Control at Reed quarry, assisted in numerous ways; Roy L. Trexler, president
of Columbia Quarry Company supplied quarry information and granted
access to the Ullin and Jonesboro quarries; Leslie A. Wright, superintendent
and J. E. Jones, office manager of Jonesboro quarry provided assistance on
quarry safety; Bernie Brust, manager, provided assistance at Ullin quarry;
and Ron Graul of Les Wilson, Inc., vice president/program director and
secretary of Illinois Geological Society (IGS) coordinated field trip logistics.
Especially appreciated is the help of the ISGS staff in the Geological
Records and Samples Library, in particular John Klitzing, Bill Revell,
Charles Zelinsky, and Anne Faber. Jacquelyn L. Hannah, graphic artist,
provided invaluable assistance.

REFERENCES

Burchette, T.P., and V.P. Wright, 1992, Carbonate ramp depositional systems:
Sedimentary Geology, v. 79, p. 3-57.

Guff, R.M., 1984, Carbonate sand shoals in the middle Mississippian (Val-
meyeran) Salem-St. Louis-Ste. Genevieve Limestones, Illinois Basin, in
P.M. Harris (ed.), Carbonate Sands - A Core Workshop: Society of Eco-
nomic Paleontologists and Mineralogists Core Workshop 5, p. 94-135.

Dever, G.R., Jr., and P. McGrain, 1969, High-Calcium and Low-Magnesium
Limestone Resources in the Region of the Lower Cumberland, Tennes-
see, and Ohio Valleys, Western Kentucky: Kentucky Geological Survey,
Series 10, Bulletin 5, 192 p.

Dunham, R.J., 1962, Classification of carbonate rocks according to depositional
texture, in W.E. Ham (ed.), Classification of Carbonate Rocks: American
Association of Petroleum Geologists, Memoir 1, p. 108-121.

Embry, A.F., III, and J.E. Klovan, 1971, A Late Devonian reef tract on north-
eastern Banks Island, Northwest Territories: Canadian Petroleum Geology,
Bulletin 19, p. 730-781.

Howard, R.H., 1991, Hydrocarbon reservoir distribution in the Illinois Basin,
in M.W. Leighton, D.R. Kolata, D.F. Oltz, and J.J. Eidel (eds.), Interior
Cratonic Basins: American Association of Petroleum Geologists, Memoir 51 ,
p. 299-327.

Lineback, J.A., 1966, Deep-Water Sediments Adjacent to the Borden Siltstone
(Mississippian) Delta in Southern Illinois: Illinois State Geological
Survey, Circular 401 , 48 p.

Lineback, J.A., and R.M., Cluff, 1985, Ullin— Fort Payne, A Mississippian shallow
to deep water carbonate transition in a cratonic basin, in P.D. Crevello and
P.M. Harris (eds.), Deep-Water Carbonates: Buildups, Turbidites, Debris
flows and Chalks: Society of Economic Paleontologists and Mineralogists
Core Workshop 6, p. 1-26.

STRATIGRAPHIC AND BIOSTRATIGRAPHIC

FRAMEWORK OF THE ULLIN LIMESTONE

("WARSAW") AND FORT PAYNE FORMATION

Rodney D. Norby

STRATIGRAPHIC NOMENCLATURE

The Ullin Limestone and Fort Payne Formation are mid-Valmeyeran in age
(late Osagean through early Meramecian). Understanding the depositional
setting for these units depends upon determining their physical relationship
with adjacent units (fig. 29). Biostratigraphy provides one key in decipher-
ing lithostratigraphic relationships (fig. 30). Detailed sequence stratigraphy
may provide another key. In this guidebook, the name Ullin Limestone or Ullin
(short form) has been employed for the equivalent unit "Warsaw," as used
by the oil industry in Illinois, and for the approximately equivalent Warsaw
Limestone, as used in Kentucky.

Ullin Limestone

The mid-Valmeyeran Ullin Limestone was named by Lineback (1966), largely
for what he described as light colored, fine to coarse grained, bryozoan- and
crinoid-rich limestones (packstones, grainstones, wackestones, and lime
mudstones of Dunham's classification [1962]) found in southern Illinois. The
upper part of the composite type section of the Ullin was described from Ullin
quarry (Stop 2). The lower part of the type section was described from natural
exposures a few miles away (Sees. 21 , 22, T14S, R1 W, Alexander County).
Most of these natural exposures have been reinterpreted (Nelson, ISGS,
personal communication 1993) to be part of the underlying Fort Payne Formation

ILLINOIS

Salem Ls.

Warsaw
Sh.

Fort

Payne

Fm.

~\ Ullin Ls.
\ ("Warsaw")

Borden \ S
SIst. \ >

Burlington- 1
Keokuk Ls. 1

[ Springville Sh.-^.

Chouteau Ls.

New Albany Gp.

INDIANA

S-C W

KENTUCKY

W-C

Salem Ls.

Harrodsburg Ls.

Borden Gp.
(fms. undiff.)

New Providence Sh.

i *

au.
a

:£

Rockford Ls.

New Albany Sh.

Salem Ls.

Warsaw Ls.

Fort

Payne

Fm.

Harrodsburg Ls.

Borden Fm.

New Providence Sh.

Rockford Ls.

Hannibal Sh.

Chattanooga Sh.

Maury Fm. equiv.

New Albany
Sh.

Figure 29 Stratigraphic terminology used in Illinois, Indiana, and Kentucky for units in field trip region. Physical
relationships are based on interpretation (this study) of the lithostratigraphy of these units as studied primarily in Illinois.

rather than the Ullin. Thus, at least locally, the thickness of the Ullin Limestone
and the relationships of the Ullin and Fort Payne need to be reassessed.

The Ullin reaches thicknesses of more than 800 feet in a small area in Hamilton
County, southern Illinois. Although the Ullin generally overlies the Fort Payne,
in some areas, it overlies the Borden, Springville, Warsaw, or Chouteau
Formations. It underlies and pinches out beneath the Salem to the west and
north in Illinois (Lineback 1 966) (figs. 32, 34).

Lineback (1966) divided the Ullin into two members, the Ramp Creek (lower)
and the Harrodsburg (upper). The boundary between the two members is
gradational and the members appear to intertongue. The names of both
members are derived from approximately equivalent formations that are rec-
ognized in western Indiana. In this guidebook, we have not formally used
these member designations because this was not our primary purpose. Our in-
formal usage of lower Ullin and upper Ullin, in general, conforms to the
named members. Until we can examine sufficient data to accurately identify the
members with confidence, we have employed this informal usage.

a. y

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UPPER MISSISSIPPI

VALLEY STANDARD

FORMATIONS

SOUTHERN ILLINOIS
(Collinson and Scott 1958;
Lineback 1966; this study)

WESTERN KENTUCKY

(Sable and Dever1990;

*this study)

SOUTHWESTERN INDIANA

(Nicoll and Rexroad 1975,

Shaver et al. 1986)

MISSISSIPPI VALLEY

CONODONT ZONES

(unrevised taxonomic and

zonal nomenclature after

Collinson, Scott and Rexroad

1962; emended by Baxter 1984)

2
<

cr
o

Salem
Limestone

Warsaw
Shale

Keokuk
Limestone

Burlington
Limestone

Fern Glen Fm

Meppen Ls

Salem
Limestone

Jones-i?r Ulhn
boro Ullin

Limestone
("Warsaw")

Borden
Siltstone

Fort

Payne

Formation

\
Springville
Shale

mulmm

Salem
Limestone

^Reed

Warsaw
Limestone

Fort Payne
Formation

vew

rovidence
Shale

Salem
Limestone

Harrodsburg
Limestone

Ramp

Creek

Formation

Muldraugh
Formation

Edwardsville Fm

Spickert Knob
Fm

New Providence
Shale

■p

Rockford Ls (part)

Taphrognathus varians-

Apatognathus

Biozone

Gnathodus texanus-

Taphrognathus

Biozone

Eotaphrus-

Bactrognathus

Biozone

Bactrognathus-

Polygnathus communis

Biozone

/ Gnathodus semiglaber-
'Pseudopolygnathus multistriatus
Biozone

Figure 30 Stratigraphic nomenclature and time correlation of units in the field trip region. Size of unit on diagram does not imply
thickness except in a very general way. The dashed lines (primarily southern Illinois column) indicate interpreted time relation-
ships from fossil evidence in Illinois, Indiana and Kentucky and on sedimentation patterns and physical relationships. Question
marks are added where no fossil evidence is available. Vertical lines indicate documented or inferred hiatuses. The vertical bars
indicate the inferred age range for rock units exposed at the Jonesboro, Ullin and Reed quarries.

"Warsaw," Warsaw Shale, and Warsaw Limestone

Before the Ullin Limestone was named, the term "Warsaw" was employed
(and still is for the most part) by the oil industry in Illinois for the limestone
package between the Salem Limestone and, in most cases, the Fort Payne
Formation.

The Warsaw Shale was named by James Hall (1857) for gray shales and
argillaceous limestones at Geode Glen near Warsaw in Hancock County,
Illinois. The Warsaw is less than 100 feet thick in the type area, but it is as much
as 300 feet thick in west-central Illinois where it consists primarily of siltstones
(a facies of the uppermost Borden). Although the Ullin Limestone can be consid-
ered a facies equivalent of part of the Warsaw Shale, Ullin is a more appropriate
name for this limestone unit in most of the subsurface of southern Illinois.

In Kentucky and Tennessee, the name Warsaw has also been used for lime-
stones with approximately the same lithologies, contacts and age as the Ullin
of Illinois. In western Kentucky, the Warsaw or "Big Light" (drillers' terminology)
is a 250 to 500 feet thick, light to medium gray biocalcirudite, biocalcarenite,
or dolomitic limestone (Sable and Dever 1990). The Warsaw thins to the east
and is about 30 feet thick in central Kentucky (Sable and Dever 1990). The type
Warsaw of Illinois is neither traceable nor lithologically similar to the Warsaw
of Kentucky and Tennessee; and although Sable and Dever (1990) suggested
the name should be abandoned for usage in Kentucky and Tennessee, they
did not indicate what name should be used in its place. They equated the
Warsaw of western Kentucky with the Ullin of Illinois and the Ramp Creek,
Harrodsburg, and Muldraugh Formations of Indiana.

For our descriptions of Reed quarry (Stop 1), we have employed Ullin terminol-
ogy, which does not equate exactly with Kentucky's usage of Warsaw Limestone
(Dever and McGrain 1969, Sable and Dever 1990). In our preliminary work,
we have drawn the Fort Payne-Ullin contact approximately 70 feet lower in
the quarry section and included the mound facies in the lower part of the Ullin.
This 70-foot transitional interval shows some of the very dark gray mudstone-
wackestone that is more typical of the Fort Payne. However, bedding char-
acteristics, fossil content and the mound facies suggest to us that it should
be allied with the Ullin.

Fort Payne Formation

The Fort Payne Formation was named by Smith (1890) for dark, very fine
grained siliceous, cherty limestones exposed near Fort Payne, northwestern
Alabama. The Fort Payne is widespread over the south-central United States
and has its northwestemmost occurrence in southeastern Illinois, where it is more
than 600 feet thick in Pope County. The formation thins to the west and north.

In western Kentucky, the Fort Payne is also a dark gray, fine grained, siliceous
and cherty limestone with planar beds. It reaches thicknesses of more than
600 feet (e.g. core from Reed quarry; see Dever and McGrain, 1969). As noted
above, approximately the upper 70 feet of the Fort Payne (as referred to by
Dever and McGrain 1969, Sable and Dever 1990) at the Reed quarry have
been included in the Ullin (this guidebook).

BIOSTRATIGRAPHY

The general age of the Ullin Limestone and Fort Payne Formation in the Illinois
Basin is moderately well established, partly on the basis of stratigraphic
position and partly on paleontologic evidence (Shaver 1985). These two units
occupy a position (fig. 30) in the middle of the Valmeyeran Series (late Osagean
through early Meramecian). Preliminary conodont microfossil information
collected during this study confirms these findings.

Age of Springville Shale (Illinois), Basal Borden Group
(Indiana), and New Providence Shale (Kentucky)

Biostratigraphic data from these underlying units are important in establishing
the age of the Fort Payne and Ullin. Data on conodonts obtained from a site
near Jonesboro, Illinois, indicate that the age of the lowest few feet of the
Springville Shale (an equivalent of at least the lowest part of the New Provi-
dence Shale of Indiana; fig. 30) is equivalent to the Fern Glen or earliest
Burlington (Collinson and Scott 1958) and within the Bactrognathus-
Polygnathus communis Biozone (Collinson et al. 1962). Collinson and Scott
(1 958) thought that the Springville in this area was overlain by the Burlington
Limestone; but later work by Lineback (1 966) indicates that the unit should
be the cherty Fort Payne. No information is available for the thicker
(about 50 ft) upper part of the Springville; it may be equivalent in age to
the Burlington (fig. 30, southern Illinois column).

In southern Indiana and north-central Kentucky, the basal part of the New
Providence Shale (the lowest unit of the Borden Group) was found to be no
older than late Burlington or even early Keokuk equivalent (fig. 30, south-
western Indiana column); Rexroad and Scott (1964) based their conclusion
on the presence of the conodonts Bactrognathus distortus and Gnathodus
texanus. Crinoids recovered from the Button Mold Knob fauna of the New
Providence Shale Member of the Borden Formation in south-central Indiana
and north-central Kentucky also indicate an age-equivalency to the Keokuk
Limestone (Kammer 1984).

Age of the Borden Siltstone (Illinois) and Main Part of the
Borden Group/Formation (Indiana/Kentucky)

Age data are not available for the Borden Siltstone in Illinois. It appears to be
slightly older than the Fort Payne and Ullin, according to its stratigraphic
position and limited fossil data from Indiana and Kentucky. The upper part of
the Borden may be the same age as the Fort Payne.

In Indiana, the conodonts Gnathodus texanus and Taphrognathus varians
were recovered from the Edwardsville Formation (Nicoll and Rexroad 1 975) and
from all three members of the Muldraugh Formation (Whitehead 1978), com-
ponents of a Borden facies that developed in an outer platform to upper slope
setting (Whitehead 1978). These conodonts represent the Gnathodus texanus-
Taphrognathus Biozone (Collinson et al. 1962), or basically an age-equivalent
of the Keokuk (fig. 30). I suggest, on the basis of conodont ranges, that it
could also be equivalent in age to the lower part of the type Warsaw Shale.
This age would apply to the latest part of the Borden complex in Indiana,
but ages could be slightly younger for the last deltaic phase in Illinois.

Several paleoenvironmental studies in west-central Indiana (Ausich et al. 1 979,
Kammer et al. 1983) involved determining the ages of the Edwardsville
Formation and several related units (delta-platform facies of the upper part of
the Borden. These upper Borden units were correlated with the Keokuk on
the basis of several crinoid and brachiopod species.

Age of the Fort Payne Formation

A Keokuk-age assignment for the Fort Payne Formation (fig. 30) is indicated
by conodont information from (1) the upper part of the Fort Payne at Reed
quarry, (2) a core (Superior Oil, Greathouse no. 30) in White County, Illinois
(fig. 2), and (3) an isolated outcrop just west of Jonesboro. The Fort Payne
in southern Illinois was previously equated, based on limited information,
with the type Warsaw (Shaver 1985, Norby 1991). No biostratigraphic
information is yet available from the lower Fort Payne of Illinois. It should be
no older than Keokuk, if the ages of the underlying units have been correctly
interpreted.

Conodont data on the type Fort Payne Formation in northwestern Alabama
(Ruppel 1971) and the strata bounding the Fort Payne in nearby areas
(Drahovzal 1 967) all indicate latest Osagean age (equivalent to the Keokuk).
A middle Osagean age is suggested for the Fort Payne in northwestern
Georgia (Ausich and Meyer 1990). In south-central Kentucky and north-
central Tennessee, Ausich and Meyer (1988) recovered a blastoid fauna from
several facies of the Fort Payne, which they equated to the Keokuk. The occur-
rence of the conodont Gnathodus texanus with the blastoids confirms this
age (Ausich and Meyer 1 988). Additional collections of crinoids from this same
area also indicate an age equivalent to the Keokuk (Ausich and Meyer 1 990).

Age of the Ullin Limestone ("Warsaw")

The Ullin Limestone has been considered to be the same age (earliest
Meramecian) as the Warsaw in its type area of western Illinois (Lineback
1966). This age is approximately correct, but the Ullin was more recently
considered to range in age from early Osagean to early Meramecian
(Shaver 1985). In a general review paper, Norby (1991) correlated the
Ullin with the lower part of the Salem.

A conodont fauna dominated by the conodont Taphrognathus varians was
reported from the Ullin (Collinson in Lineback 1966). Nicoll and Rexroad
(1 975) reported this same fauna from the upper part of the Ramp Creek and
Muldraugh and also in the Harrodsburg and Salem Limestones in Indiana.
Both reports suggested an age equivalent to the Warsaw. Samples from this
study corroborate these reports and indicate an early Meramecian age for
the upper part (Harrodsburg Member) of the Ullin in Illinois (equivalent to
either the upper part of the type Warsaw or, more likely, the lower part of the
Salem). The lower part of the Ullin in Illinois appears to be no older than the type
Warsaw equivalent, although no fossil information is specifically available for
the lower part of the Ullin. The age of the Ullin ("Warsaw") in the subsurface
of Illinois is probably equivalent to the type Warsaw, although parts could
be slightly younger. In areas of thick Ullin (600 ft or more), the lower part of the
Ullin could be older than the type Warsaw (fig. 30), although this has not
been verified biostratigraphically.

The Warsaw Limestone as used in western Kentucky appears to be the same
age as the type Warsaw (western Illinois) from preliminary microfossil data
recovered in this study.

Sedimentological models suggest a lateral intertonguing of at least part of the
Ullin with the Fort Payne (Lasemi, this guidebook). Fossil data from thicker
subsurface sections might corroborate this model. No conodont data are
presently available, however, for the deeper parts of the Illinois Basin where
a thicker Fort Payne-Ullin interval occurs.

REFERENCES

Ausich, W.I., T.W. Kammer, and N. G. Lane, 1979, Fossil communities of the
Borden (Mississippian) delta in Indiana and northern Kentucky: Journal
of Paleontology, v. 53, no. 5, p. 1182-1196.

Ausich, W.I., and D.L. Meyer, 1988, Blastoids from the late Osagean Fort
Payne Formation (Kentucky and Tennessee): Journal of Paleontology,
v. 62, p. 269-283.

Ausich, W.I., and D.L. Meyer, 1990, Origin and composition of carbonate
buildups and associated facies in the Fort Payne Formation (Lower
Mississippian, south-central Kentucky): An integrated sedimentologic and
paleoecologic analysis: Geological Society of America Bulletin, v. 102,
p. 129-146.

Baxter, S., 1984, The Eotaphrus-Bactrognathus Zone, a new name for a cono-
dont zone from the type Burlington Formation: Neuvieme Congres Interna-
tional de Stratigraphie et de Geologie du Carbonifere (Washington and
Champaign-Urbana 1979), Compte Rendu, v. 2, p. 247-252.

Collinson, C, and A.J. Scott, 1958, Age of the Springville Shale (Mississippian)
of Southern Illinois: Illinois State Geological Survey, Circular 247, 12 p.

Collinson, C, A.J. Scott, and C.B. Rexroad, 1962, Six Charts Showing
Biostratigraphic Zones and Correlations Based on Conodonts from
the Devonian and Mississippian Rocks of the Upper Mississippi Valley:
Illinois State Geological Survey, Circular 328, 32 p.

Dever, G.R., Jr.,and P. McGrain, 1969, High-Calcium and Low-Magnesium
Limestone Resources in the Region of the Lower Cumberland, Tennessee,
and Ohio Valleys, Western Kentucky: Kentucky Geological Survey, Series 10,
Bulletin 5, 192 p.

Drahovzal, J. A., 1967, The biostratigraphy of Mississippian rocks in the
Tennessee Valley, in A Field Guide to Mississippian Sediments in Northern
Alabama and South-Central Tennessee: Alabama Geological Society,
5th Annual Field Trip Guidebook, p. 10-24.

Dunham, R.J., 1962, Classification of carbonate rocks according to deposi-
tional texture, in W.E. Ham (ed.), Classification of Carbonate Rocks:
American Association of Petroleum Geologists, Memoir 1, p. 108-121.

Hall, J., 1857, Observations upon the Carboniferous limestones of the
Mississippi Valley (abs.): American Journal of Science, v. 23, p. 187-203.

Kammer, T.W., 1984, Crinoids from the New Providence Shale Member of
the Borden Formation (Mississippian) in Kentucky and Indiana: Journal
of Paleontology, v. 58, no. 1 , p. 1 1 5-1 30.

Kammer, T.W., W.I. Ausich, and N.G. Lane, 1983, Paleontology and
stratigraphy of the Borden delta of southern Indiana and northern
Kentucky, in R.H. Shaver and J. A. Sunderman (eds.), Field Trips in Mid-
western Geology: Bloomington, Indiana, Geological Society of America,
Indiana Geological Survey and Indiana University Department of Geology,
v. 1, field trip 2, p. 37-71.

Lineback, J.A., 1966, Deep-Water Sediments Adjacent to the Borden Siltstone
(Mississippian) Delta in Southern Illinois: Illinois State Geological Survey,
Circular 401 , 48 p.

Nicoll, R.S., and C.B. Rexroad, 1975, Stratigraphy and Conodont Paleontology
of the Sanders Group (Mississippian) in Indiana and Adjacent Kentucky:
Indiana Geological Survey, Bulletin 51 , 45 p.

Norby, R.D., 1991, Biostratigraphic zones in the Illinois Basin, in M.W.
Leighton, D.R. Kolata, D.F. Oltz, and J.J. Eidel (eds.), Interior Cratonic
Basins: American Association of Petroleum Geologists, Memoir 51,
p. 179-194.

Rexroad, C.B., and A.J. Scott, 1964, Conodont Zones in the Rockford Lime-
stone and the Lower Part of the New Providence Shale (Mississip-
pian) in Indiana: Indiana Geological Survey, Bulletin 30, 59 p.

Ruppel, S.C., 1 971 , Conodont biostratigraphy and correlation of the Fort
Payne Chert and Tuscumbia Limestone (Mississippian) at selected sites in
northwestern Alabama: Masters thesis, University of Florida, Gainesville, 74 p.

Sable, E.G., and G.R. Dever, Jr., 1990, Mississippian Rocks in Kentucky:
U. S. Geological Survey, Professional Paper 1503, 125 p.

Shaver, R.H. (coordinator), 1985, Midwestern basin and arches region (chart),
in F.A. Lindberg (ed.), Correlation of Stratigraphic Units of North Amer-
ica: American Association of Petroleum Geologists COSUNA Chart
Series, columns 8-10.

Shaver, R.H., C.H. Ault, A.M. Burger, D.D. Carr, J.B. Droste, D.L. Eggert,
H.H. Gray, D. Harper, N.R. Hasenmueller, W.A. Hasenmueller,
A.S. Horowitz, H.C. Hutchison, B.D. Keith, S.J. Keller, J.B. Patton,
C.B. Rexroad, and C.E. Wier, 1986, Compendium of Paleozoic Rock
Unit Stratigraphy in Indiana - A Revision: Indiana Geological Survey,
Bulletin 59, 203 p.

Smith, E.A., 1890, Geological structure and description of the valley regions
adjacent to the Cahaba coal field, in Report on the Cahaba Coal Field:
Alabama Geological Survey, part 2, p. 137-180.

Whitehead, N.H., III, 1978, Lithostratigraphy, depositional environments, and
conodont biostratigraphy of the Muldraugh Formation (Mississippian) in
southern Indiana and north-central Kentucky: Southeastern Geology, v. 19,
p. 83-109.

WAULSORTIAN MOUND, BRYOZOAN BUILDUP,

AND STORM-GENERATED SANDWAVE FACIES

IN THE ULLIN LIMESTONE ("WARSAW")

Zakaria Lasemi

OVERVIEW OF WAULSORTIAN MOUNDS

The early to early mid-Mississippian (late Tournaisian to early Visean) is char-
acterized by widespread distribution of carbonate mud mounds in various
regions in North Africa, Europe, and North America (Wilson 1975, Bolton et
al. 1982, West 1988, Lees 1988). These mounds are generally known as
Waulsortian mud or reef mounds after the village of Waulsort in the Dinant
Basin of Belgium. They are quite variable in thickness and distribution. In
Ireland, for example, the mounds are more than 3,000 feet thick and coalesced
into large banks covering tens of thousands of square miles (Lees 1 961 ,
Sevastopulo 1982).

Facies

Waulsortian mounds vary in shape from lenticular bodies in shallower areas
to steep mounds, commonly with slopes of 10° to 50°, in outer ramp to basin
environments. Lime mudstone to wackestone with scattered fenestrate
bryozoans and crinoids characterizes the core facies of these mounds. The
mound core is generally massive to crudely bedded (possibly because of
vertical accretion) and may contain sparry calcite-filled cavities generally
known as stromatactis (Bathurst 1982).

In general, flanking facies of Waulsortian mounds are well bedded crinoidal to
crinoidal-bryozoan wackestone to grainstone. The intermound facies, typically
well bedded, includes siliceous and cherty carbonates that are generally dark
and argillaceous. In some areas, crinoid-bryozoan packstone to grainstone
may be an important component of the intermound facies. These coarser
intermound facies represent debris apron deposits formed by off-mound
transport of skeletal debris.

A Waulsortian mound complex is generally overlain by a packstone to grain-
stone facies, which may be storm -gene rated skeletal sandwaves (Lasemi et
al. 1994a, b) or oolitic limestone of the overlying units. Some mounds are
capped by deeper water limestone and shale, indicating a drowning event
(Precht and Shepard 1989) that terminated mound development.

North American Waulsortian-type mounds are generally similar to those in
Europe except that, in many areas, the core facies appears to be generally
thinner and the flanking facies is thicker bryozoan and crinoid grainstone. Also,
in situ bryozoan-dominated bafflestone buildups, which are developed on the
crest and flanks of mounds, appear to be a characteristic feature of some
mounds, such as those in the Illinois Basin (Lasemi et al. 1994a, b and this
study). Similar buildups may be present in other North American mounds (Ahr
and Ross 1982, Davies et al. 1989) but have been interpreted, perhaps erro-
neously, by those authors to represent the core facies of Waulsortian-type

mounds. The Ullin mounds in the Illinois Basin are also distinguished from
those reported in Europe and other regions in North America by an abun-
dance of chert bands and nodules (fig. 14), possibly representing former
cavities similar to stromatactis.

Source of Micrite

The source of the micrite that constitutes the core facies of Waulsortian
mounds is controversial. Baffling and trapping of transported carbonate
mud by bryozoans and crinoids (Pray 1958, Wilson 1975, Philcox 1967) and
trapping and binding by organic mats, probably blue green algae (Pratt 1982),
have been suggested as possible mechanisms for mound development. Lees
and Miller (1985) questioned these interpretations based on the rare
occurrences of baffling organisms in some mounds, the large size of many
mounds, and textural and compositional differences in the mound core and
intermound and flanking facies. They suggested that the carbonate mud for
mound growth may have been formed in situ by microbially induced (i.e. by
bacteria and cyanobacteria) precipitation. A similar origin was also suggested
by Monty et al. (1982) and Tsien (1985) for the lime mudstone in some
Devonian mud mounds.

Distribution of Mounds

In some areas, structure is a possible control on the development of Waul-
sortian mounds. There is evidence for block faulting and subsidence in
several areas where Waulsortian mounds have developed (Wilson 1975,
Miller and Grayson 1982). Miller and Grayson (1982) suggested a tilted block
fault model for the development of a ramp-like depositional setting in the
Lower Carboniferous units of England. In this model, Waulsortian mounds
developed on the deeper, downthrown side of the fault. Some mounds show a
linear arrangement, either parallel to but some distance from an anticlinal axis,
or on the downthrown side of a block fault (Wilson 1975). However, some
mounds regarded by Wilson (1975) as Waulsortian are younger, perhaps shelf
margin-type reefs (Lees 1988).

Waulsortian mounds are, for the most part, randomly distributed on ramps and
do not form a shelf slope break (Ahr 1989). They are generally initiated
downslope on ramps and in basinal settings below storm wave base in deeper
water environments. Mounds in basinal settings developed into vertically
stacked buildups similar to pinnacle reefs. Others, such as those in Ireland
(Sevastopulo 1982, Lees 1961), accreted laterally into complex banks
thousands of square miles across. A deeper water origin of the mounds is
indicated by the lack of shallow water indicators such as calcareous green
algae, coated grains, and subaerial exposure features. Additional evidence
for a deeper water origin includes the (1 ) smooth geometry of the mounds with
no channel or spur and grooves, (2) deeper water origin of the equivalent and
enclosing carbonate and shale (some with pelagic fauna), and (3) overall
paleogeographic position (Wilson 1975). During the later stages of their
development, some mounds may have built up into the photic zone, as indi-
cated by the appearance of coated grains, green algae, and micritization
(Lees and Miller 1985).

A depth-related facies distribution for Waulsortian mounds (fig. 31) has been
developed by Lees and Miller (1985), who based their interpretaton on the
relative abundance of readily recognizable skeletal allochems and the presence
or absence of green algae and coated grains:

A. fenestellid-bryozoan facies with abundant fenestellid sheets and
calcite-filled cavities or stromatactis,

B. siliceous sponge facies,

C. sponge/cyan op hytes (calcimicrobes) facies,

D. skeletal algae and coated grain facies.

Facies A-C are characteristic of subphotic zones, whereas facies D only
developed in the photic zone. Because of their depth-dependence, not all
facies may be present in any one place. After examining the paleontological
data, Lees and Miller (1985) suggested various water depths for different
facies of the Belgian mounds (type area): greater than 500 feet (facies A),
400 to 500 feet (facies B), 300 to 400 feet (facies C), and less than 300 feet
within the photic zone (facies D).

The development and disappearance of Waulsortian mounds during the
early to mid-Mississippian Period is neither well understood nor within the
scope of this study. A combination of factors such as tectonism, sea-level
rise, and changes in ocean circulation patterns may have been involved. Late

Waulsortian mound
(Mississippian)

Si 400 m
approximate scale

facies D

facies C

facies B

facies A

photic
subphotic

sea level

photic
subphotic

Figure 31 Facies distribution and depth zonation of Waulsortian mounds: Vertical
succession (top left) in a Belgian Waulsortian mound (type area); ecological assem-
blages and depth zonation (top right): distribution of Waulsortian facies on a carbonate
ramp (inset). (Modified from James and Bourque [1992] and Lees and Miller [1985].)

Devonian to early Visean (mid-Mississippian) was a unique time, characterized
by several tectonic, oceanographic, and biological events on a worldwide
scale. There were nearly synchronous, relatively rapid increases in the rates
of subsidence of most preexisting margins and basins of North America
(Kominz and Bond 1991). Tectonic subsidence modeling for the Illinois
Basin (Treworgy et al. 1991) indicates a subsidence rate increase around
mid-Mississippian time.

Major expansion of the oxygen-minimum zone in the ocean during the late
Devonian to early Mississippian resulted in widespread development of anoxic
conditions (Jenkyns 1986), which may have contributed to deposition of
organic-rich black shales (e.g. the New Albany). A major faunal extinction at
the end of the Devonian effectively eliminated the frame-building organisms
responsible for reef construction. Early to early mid-Mississippian was also a
time for the development of widespread carbonate ramp settings (Ahr 1989).
Mud mounds became widespread and developed in deeper water settings
downslope on such ramps or within basins (Wilson 1975). The distribution of
ramps and mud mounds at this time may be related to continuous subsidence
and slow recovery of frame builders after the end of the Devonian (West 1 988),
and shifting of the carbonate factory into a deeper offshore setting (Wright
and Faulkner 1990).

Hydrocarbon Production from Waulsortian Mounds

Waulsortian mounds are prolific hydrocarbon reservoirs in several regions
of North America. Hydrocarbon production is mainly from porous flanking
packstone and grainstone and, less commonly, from fractured and dolomitized
core fades of the mounds. The mounds are generally surrounded by or grade
into a deeper water facies that is usually dark and, in places, organic-rich.
Because of high porosity in flanking beds and proximity to relatively organic-rich
rocks, Waulsortian mounds have excellent potential for reservoir development
where permeable. Vertically stacked facies in some mounds are sites for
development of multistory reservoirs. The dense core facies is an effective
barrier for hydrocarbon entrapment in vertically stacked mounds. Waulsortian
mounds are productive in Illinois (Lasemi et al. 1994a, b), Kentucky and
Tennessee (MacQuown and Perkins 1982), north-central Texas (Ahr and
Ross, 1982), and north-central Alberta (Morgan and Jackson 1970, Davies et
al. 1989). Drilling by Conoco in the Mississippian Lodgepole Formation in
North Dakota encountered a prolific reservoir in a Waulsortian-type mound.
Initial production was greater than 2,000 barrels of oil per day and 1 .2 million
cubic feet of natural gas per day (Burke and Diehl 1993).

ULLIN ("WARSAW") AND FORT PAYNE FORMATIONS

Previous Studies

According to Lineback (1966, 1969), the lower Valmeyeran carbonate and
clastic units in the Illinois Basin may have formed during four separate deposi-
tional events:

1 . Deposition of the Burlington-Keokuk Limestones and the underlying
Fern Glen apparently occurred on a carbonate shelf adjacent to a
relatively deep, starved basin (Lineback 1981) (figs. 32, 33). A similar

HAROLD C.SANDERS

Harrison no. 1

T15N-R5E-Sec 22 SW NW SE

Moultrie Co., IL

B'
LLOYD A. HARRIS

Ryan no. 4

T21N-R3E-Sec 21 C S1/2 SW SW

De Witt Co., IL

Figure 32 South-north cross section (B-B') from Moultrie County to De Witt County, Illinois (see fig. 2 for location). Note rela-
tionship of Borden, Fern Glen, Burlington and Keokuk Formations (from Treworgy et al., in review).

depositional setting was apparently present at the same time in other
regions of North America and western Europe (Lane 1978).
2. According to Lineback (1981), deposition of the Burlington-Keokuk
Limestone in the Illinois Basin was terminated by a tongue of the Borden
delta, which extended westward into Illinois and then was deflected
southward by the bank margin topography (fig. 33).
3-4. Later, the Fort Payne (3) and then the Ullin (4) filled the deeper water
areas remaining after cessation of Borden sedimentation (fig. 34).

absent

Figure 33 Thickness of early Valmeyeran deltaic sediments (after Lineback, 1966). Note east
edge of Burlington-Keokuk bank.

In a more recent study, Lineback and Guff (1985) suggested that the Ullin
and Fort Payne Formations were laterally gradational. They suggested that
the Ullin was deposited on a ramp in "structurally higher" parts of the La Salle
Anticlinorium and graded downslope into deeper water carbonates of the Fort
Payne. They further suggested that the thick areas of the Ullin in the central
part of the basin represent carbonates transported from these structurally
higher, shallower areas. We agree with the gradational nature of the Ullin and
Fort Payne (fig. 34) and an overall ramp depositional setting; however, we do
not believe that the source of Ullin carbonates is limited to structurally higher,
shallower areas. Presence of relatively well-preserved, delicate bryozoans
that constitute the bulk of the bafflestone facies commonly found within the
Ullin in these areas indicates in situ development.

Depositional Environment

Various facies of the Ullin and Fort Payne observed in quarry exposures inter-
grade laterally, forming a facies belt characteristic of a carbonate ramp setting
(fig. 4). (For a review of the ramp settings, see Burchette and Wright 1992.)
Development of Waulsortian-type mounds represents the early stages of car-
bonate deposition on this ramp after transgression of the Fort Payne sea. The
lithologic character of the Fort Payne represents a deeper water basinal
facies, as suggested by Lineback and Guff (1985), and is similar to deep water
carbonates reported from other regions (Wilson 1969, Smith 1977). Deposi-
tion below the photic zone is indicated by the absence of calcareous
green algae and micritized grains both in the Ullin (except in the uppermost
part) and in the Fort Payne carbonates. Lack of storm-generated sedimentary
structures within the mound facies indicates that the mounds in the Ullin
developed below storm wave base.

The interpretation of a ramp depositional setting for the Ullin— Fort Payne is
supported by (1) an apparent lack of evidence for shelf edge reef or shoal
(Lineback and Guff 1985), and (2) the absence of soft sediment deformation
features and carbonate breccia, both indicative of a shelf-slope break. A ramp
depositional model for the Ullin— Fort Payne is also consistent with widespread
ramp development during early to early mid-Mississippian time (Ahr 1989).

Lineback and Guff (1985) suggested that local thick areas of the Ullin Lime-
stone may represent only local development of Waulsortian mounds. We
conclude that these mounds, along with in situ bryozoan buildups, were
prevalent and coalesced laterally and vertically, forming several large carbon-
ate banks (20 miles wide by up to 70 miles long; fig. 35) surrounded by the
deep-water Fort Payne (Lasemi et al. 1994b and work in progress; fig. 36).
This conclusion is supported by the reciprocal thickness relationship of the
Fort Payne and Ullin (figs. 35, 36) and by the presence of Waulsortian-type
mounds and bryozoan-dominated buildups in the quarry exposures of the
Ullin. The Ullin mounds, which died out in the early Meramec (early Visean),
represent the latest stage in the worldwide development of the Waulsortian
mounds. Their disappearance in Illinois may relate to a gradual shallowing of
the marine environment caused by vertical aggradation of carbonates and a
decrease in the rate of subsidence.

There appears to be two general types of mound-like carbonate deposits in
the Ulllin Limestone in Illinois. One type (figs. 4a, 6, 7, 1 1 ) is similar in part to

UNOCAL

Cisne Comm. no. 1

T1S-R7E-Sec3SWNENE

Wayne Co., IL

ishsls-

ishsls -

TAMMARACK

Brach no. 1

T1S-R7E-Sec3

NW NE NW

H-A-V-E OIL CO.

Sutton no. 1

T3N-R5E-Sec 1 C NW NE

Clay Co., IL

Figure 34 South-north cross section (A-A') from Wayne County to Effingham County, Illinois
(see fig. 2 for location). Note relationship of Borden, Fort Payne, and Ullin ("Warsaw") Formations
(from Treworgy et al., in review).

ATLAS ENERGY CORP.

Thompson-Wetherell Comm. no. 1

T9N-R5E-Sec 20 NE NW NW

Effingham Co., IL

many Waulsortian mounds recognized in Europe, south-central Kentucky,
Tennessee, and other regions in North America (Lees 1988, Precht and
Shepard 1989, Ausich and Meyer 1990, MacQuown and Perkins 1982; see
also reviews in Wilson 1975 and Bolton et al. 1982). The other type of mound-
like deposit observed in the Ullin appears to be a lenticular, skeletal sand
(grainstone) pile (figs. 19-21).

Both the Waulsortian -type mound and lenticular skeletal sand piles in the
Ullin were the preferred sites for the development of in situ bryozoan and

Figure 35 Thickness of the Ullin Limestone ("Warsaw") (after Lineback, 1966). Note highlighted
areas of thick Ullin.

crinoid bafflestone buildups (figs. 4a, 22a-b, 23). Data from cores and drill
cuttings indicate that such buildups, especially those bryozoan-dominated,
constitute a major portion of the Ullin Limestone in Illinois (figs. 4, 22b). They
developed on the crest and the flank of carbonate mounds and provided a
source for skeletal sands that were deposited as debris aprons in intermound
areas and as storm -gene rated sandwaves in mid-ramp settings. Vertical ac-
cretion and lateral progradation of various facies of the Ullin, along with a de-
crease in the rate of subsidence, resulted in a shallowing-upward ramp setting,

! ;

i ■ ■

LI IN

Valmeyeran

absent

Wr r*

L n J L

X X

' ._ J

, V^

../' .

Figure 36 Thickness of the Fort Payne Formation (after Lineback, 1966). Note highlighted
areas with no Fort Payne.

which eventually ended extensive mound development during deposition of
the upper Ullin (fig. 4b). A gradual shallowing is supported by the appearance
of ooids, calcareous green algae (dasyclads), and micritized grains in the up-
permost part of the Ullin. Frequent storm events resulted in widespread
sandwave development. Shallow water settings were unfavorable sites for fur-
ther development of thick Waulsortian mud mounds; however, thinner, more
isolated mud mounds and mound-like grainstone piles provided the neces-
sary high that supported the development of in situ bryozoan-dominated
patch reefs in the upper part of the Ullin. These mounds, together with the
sandwaves, formed an irregular topography (fig. 4b) that led to the develop-
ment of oolitic grainstone shoals during deposition of the overlying Salem
Limestone.

Waulsortian-type mounds of the lower Ullin The carbonate mud mound
in Reed quarry contains fenestrate bryozoan sheets, scattered crinoidal debris,
fenestrate bryozoan hash, calcified sponge spicules, and rare ostracods
(fig. 13). The presence of sponge spicules is the basis for interpreting the
mound in Reed quarry to be comparable to facies B of the Waulsortian
mounds (fig. 4a) recognized by Lees and Miller (1985) (fig. 31). Paleontological
data suggest that the water depth in which the facies B of Waulsortian mounds
developed was about 400 to 500 feet deep (Lees and Miller 1 985). Various
facies of these mounds grade laterally into the basinal submound facies of
the Fort Payne — evidence for a deeper water, outer-ramp setting for the
development of the Ullin mound in Reed quarry (fig. 4a). The deeper-water
setting of these mounds was not favorable for the development of the flanking
bryozoan bafflestone reservoir facies, as observed in the Ullin quarry.

Examination of samples from two cores (ISGS Miller nos.1 and 2) from a
location about 12 miles east of the Ullin quarry (fig. 2) revealed lithologic
characteristics suggestive of a Waulsortian-type mound. The core facies of
the mound is a lime mudstone to wackestone with scattered bryozoans and
crinoids (figs. 37, 38). The mound facies is flanked by a porous bryozoan
bafflestone facies similar to that in the Ullin quarry (see section under "Stop
Descriptions"). Thin section petrography of the core facies shows the presence
of scattered fenestrate bryozoan hash and crinoids (figs. 37, 38). Part of this
facies also has a peloidal (clotted) texture and contains rare gastropods, forams,
and ostracods (fig. 38). The skeletal allochems in this facies resemble those
in facies C (fig. 31) of Waulsortian mounds recognized by Lees and Miller
(1 985). This facies developed upramp from facies B, as it appears in Reed
quarry (fig. 4a), in a relatively shallower water setting. Lees and Miller (1 985)
suggested a depth range of about 300 to 400 feet for this facies. The water
depth here was apparently shallow enough for the development of a bryozoan
bafflestone reservoir facies on this mound (figs. 4a, 19, 22a).

Facies D (fig. 31 ) of Lees and Miller (1 985) is characterized by the presence
of calcareous green algae and micritized and coated grains. Thus far, it has
not been found in the three Illinois and Kentucky quarries; however, it may be
present in the upper Ullin in the subsurface. Brown and Dodd (1990) reported
a similar facies in the Harrodsburg Limestone and Ramp Creek Formation in
southern Indiana and northern Kentucky; however, the mounds that they
described are much smaller (4 inches to 7 feet thick) than those we have
found within the upper Ullin in the subsurface of Illinois.

Figure 37 Thin section photomicrograph (cross-polarized light) of the lime
mudstone core facies of a Waulsortian-type mound in the Ullin ("Warsaw")
from a core (ISGS Miller no. 1) taken about 12 miles east of Ullin quarry,
Illinois. Note fenestrate bryozoan frond and scattered crinoid fragments.
Black particles are pyrite. Bar scale = 1 mm.

Figure 38 Thin section photomicrograph (plane light) of the wackestone core
facies of a Waulsortian-type mound (from the same location as in fig. 36).
Note fenestrate bryozoan hash, scattered crinoids, a echinoderm spine (e),
a gastropod (g), a foram (f) and ostracods (o). Note clotted texture of the
matrix, especially in bottom left of the photomicrograph. Note also a cal-
cite-filled microfracture. Bar scale = 1 mm.

Lenticular grainstone piles of the lower Ullin The lenticular mounds in
Ullin quarry have a fine grained, grainstone core facies (fig. 21), indicating
that they are not Waulsortian-type mounds. Rather, they appear to be current-
deposited bryozoan-crinoid sand piles. This interpretation is supported by the
lack of lime mudstone matrix, moderate grain sorting, and in some cases, the
presence of current lamination. Mound-like geometry and fine grain size sug-
gest that the environment of deposition for this facies was in deeper water
than the depositional environment for the overlying sandwave facies. The
presence of relatively well preserved, flanking bryozoan bafflestone buildups
(figs. 4a, 19, 22a) indicates that these mound-like grainstones were favorable
areas for the establishment of bryozoan communities.

Sandwave facies of the upper Ullin The late stage in the evolution of the
Ullin depositional environment (fig. 4b) is represented by this facies, which
grades laterally in an upramp direction from (1) a distal facies consisting
of isolated sandwaves interfingering with lime mudstone intersandwaves in
Reed quarry, (2) an intermediate facies consisting of isolated sandwaves and
finer grained packstone to grainstone intersandwaves in Ullin quarry, to (3) a
proximal facies consisting of coalesced sandwaves of coarse grained, bryozoan-
crinoid grainstone in Jonesboro quarry (fig. 4b). This facies relationship
indicates a progressive decrease in water depth and an increase in current
energy shoreward, as suggested by a relative decrease in mud content and
an increase in grain size. Hummocky cross stratification (fig. 27) and the lack
of evidence for persistent current reworking (e.g. the lack of ooids and poor
rounding) suggest that the sandwaves were deposited by storm currents in a
mid-ramp setting below normal wave base. Repeated graded bedding, a com-
mon feature within the coalesced sandwaves in the upper Ullin in Jonesboro
quarry, probably represents multiple storm events. Storm-generated
sandwaves, which are common in modern carbonate environments such as
the Bahamas (Hine 1977), have also been documented from various ramp
settings in the Phanerozoic system (Aigner 1985, various articles in Einsele
and Seilacher 1982).

RESERVOIR POTENTIAL

OF THE ULLIN LIMESTONE ("WARSAW")

The Ullin ("Warsaw") reservoir facies is mainly a bryozoan-dominated baffle-
stone (figs. 19, 20, 22a, 23) developed on the flanks and crests of Waulsortian-
type mud mounds or on transported skeletal sand piles (fig. 4a). Subsurface
geology and petrography reveal this porous bryozoan bafflestone facies at
various horizons (some with oil shows) within the Ullin (figs. 4, 22b). Hydro-
carbon production thus far has been limited to bryozoan bafflestone buildups
(bryozoan patch reefs) and possibly storm-generated sandwaves in the up-
per Ullin. The Waulsortian mound facies in the lower Ullin has not, to our
knowledge, been tested. The production of hydrocarbons from similar
mounds in other regions of North America has been prolific, therefore the
Ullin mound facies may also be potential reservoirs. Oil shows in cuttings
from the porous facies of Ullin mounds support this hypothesis.

Petrographic examination shows excellent preservation of primary intra- and
interparticle porosity within the bryozoan bafflestone buildups (figs. 22, 23).

The generally stable original mineralogy (low-magnesium calcite) prevented
extensive dissolution-reprecipitation and occlusion of pores. Furthermore,
the stable mineralogy and minor early marine cementation prevented later
compaction and burial diagenesis. There appears to be a general relationship
between the abundance of crinoidal fragments and porosity: a decrease in
porosity corresponds to an increase in crinoidal material because of preferen-
tial cementation by syntaxial calcite (figs. 23, 39).

The porous facies of the Ullin is generally mud-free, thus contributing to a
higher reservoir permeability. Acid stimulation is probably an effective method
of increasing permeability in the bryozoan-rich facies because the microporous
nature of bryozoans generates abundant surface area for acid reaction. This
property makes the Ullin an excellent source of the carbonate used in "scrub-
ber" systems for desulfurization of coal (see Harvey, this guidebook).

Some Ullin reservoir facies, although porous, may have little permeability.
This condition is common when some micrite is present or cementation has
occurred. Under such conditions, the presence of microfractures can enhance
permeability (Tom Partin, consultant, personal communication 1994). Exami-
nation of drill cuttings and cores indicates that calcite-filled microfractures are
common in various facies of the Ullin (figs. 15, 38). Some microfractures are
oil-stained. Microfractures were apparently open during migration of petroleum,
but were filled later by calcite precipitation and cementation. Where saturated
with oil, however, microfractures remained open, thus increasing reservoir
permeability in some Ullin plays.

Figure 39 Thin section photomicrograph (cross-polarized light) of a core
sample from White County (Superior Oil , Greathouse no. 30, NE SW NE
Sec. 4-T5S-R14W), Illinois. This is a bryozoan-crinoid grainstone from the
inferred sandwave facies of the upper Ullin ("Warsaw"). Note occlusion of
pores in the more crinoid-dominated areas because of preferential overgrowth
cementation by calcite. Inter- and intraparticle porosity (black) is preserved in
bryozoan-dominated areas. Bar scale = 1 mm.

The distribution of the porous bryozoan facies may be local in some areas,
as observed in the Ullin quarry. This may be part of the reason for high initial
production occurring with very short flow time in some Ullin plays. However,
laterally and vertically extensive mounds and sandwaves with reservoir quality
facies occur in many areas of the basin (Lasemi, work in progress) and provide
excellent potential for hydrocarbon production.

Preliminary data from core samples and cuttings indicate the presence of an
argillaceous lime mudstone to wackestone at the base of the Salem Limestone
in many areas (fig. 3). Dense lime mudstone and wackestone facies (usually
the mound core facies) are also common in the upper Ullin (fig. 3) and gener-
ally cap the porous bryozoan-dominated facies of an underlying mound. The low
permeability mudstones and wackestones can effectively seal hydrocarbons
within the Ullin Limestone. The presence of these seals, high porosity, and
proximity to potential source rocks (New Albany and possibly Fort Payne)
indicate that the Ullin Limestone ("Warsaw") has great reservoir potential
throughout the basin. This is confirmed by recent discoveries of prolific petroleum-
producing zones within the Ullin Limestone in Wayne and White Counties in
Illinois.

REFERENCES AND SELECTED READINGS

Ahr, W.M., 1989, Sedimentary and tectonic controls on the development of
an early Mississippian carbonate ramp, Sacramento Mountains area, New
Mexico, in P.D. Crevello, J.L. Wilson, J.F. Sarg, and J.F. Read (eds.),
Controls on Carbonate Platform and Basin Development: Society of Eco-
nomic Paleontologists and Mineralogists, Special Publication 44, p. 203-212.

Ahr, W.M., and S.L. Ross, 1982, Chappel (Mississippian) biohermal reservoirs
in the Hardeman Basin, Texas: Transactions, Gulf Coast Association of
Geological Societies, Baton Rouge, LA, v. 32, p. 187-193.

Aiger, T., 1985, Storm depositional systems, dynamic stratigraphy in modern
and ancient shallow-marine sequences, /nG.M. Friedman, H.J. Neugebauer,
and A. Seilacher (eds.), Lecture Notes in Earth Sciences, number 3:
Springer-Verlag, Berlin, 174 p.

Ausich, W.I., and D.L. Meyer, 1990, Origin and composition of carbonate
buildups and associated facies in the Fort Payne Formation (Lower Missis-
sippian, south-central Kentucky): An integrated sedimentologic and paleo-
ecologic analysis: Geological Society of America Bulletin, v. 102, p. 129-146.

Bathurst, R.G.C., 1982, Genesis of stromatactis cavities between submarine
crusts in Palaeozoic carbonate mud buildups: Journal of the Geological
Society of London, v. 1 39, p. 1 65-1 81 .

Bolton, K., H.R. Lane, and D.V. LeMone (eds.), 1982, Symposium on the
Paleoenvironmental Setting and Distribution of the Waulsortian Facies: El
Paso Geological Society and the University of Texas at El Paso, 202 p.

Brown, M.A., and J.R. Dodd, 1990, Carbonate mud bodies in Middle Missis-
sippian strata of southern Indiana and northern Kentucky: End members
of a Middle Mississippian mud mound spectrum?: Palaios, v. 5, p. 236-243.

Burchette, T.P., and V.P. Wright, 1992, Carbonate ramp depositional systems:
Sedimentary Geology, v. 79, p. 3-57.

Burke, R., and P. Diehl, 1993, Waulsortian mounds and Conoco's new
Lodgepole well: North Dakota Geological Survey Newsletter, v. 20, no. 2,
p. 6-17.

Davies, G.R., D.E. Edwards, and P. Flach, 1989, Lower Carboniferous
(Mississippian) Waulsortian reefs in the Seal area of north-central Alberta,
in H.H.J. Geldsetzer, N.P. James, and G.E. Tebbutt (eds.), Reefs, Canada
and Adjacent Areas: Canadian Society of Petroleum Geologists, Memoir 13,
p. 643-648.

Einsele, G., and A. Seilacher (eds.), 1982, Cyclic and event stratification:
Springer-Verlag, Berlin.

Flugel, E., and E. Flugel-Kahler, 1992, Phanerozoic reef evolution: Basic
questions and data base: Fades, v. 26, p. 167-278.

Hine, A.C., 1977, Lily Bank, Bahamas: History of an active oolite sand shoal:
Journal of Sedimentary Petrology, v. 47, p. 1554-1582.

James, N.P., and P.A. Bourque, 1992, Reefs and mounds, in R.G. Walker,
and N.P. James (eds.), Fades Models: Geological Association of Can-
ada, Waterloo, p. 323-347.

Jenkyns, H.C., 1986, Pelagic environments, inG. Reading, (ed.), Sedimentary
Environments and Fades: Blackwell Scientific, Oxford, p. 343-397.

Kominz, M.A., and G.C. Bond, 1991, Unusually large subsidence and sea-level
events during middle Paleozoic time: New evidence supporting mantle
convection models for supercontinent assembly: Geology, v. 19, p. 56-60.

Lane, H.R., 1978, The Burlington Shelf (Mississippian, north-central United
States): Geologica et Palaeontologica, v. 12, p. 165-176.

Lasemi, Z., J.D. Treworgy, and R.D. Norby, 1994a, Development of Waulsor-
tian mounds and hydrocarbon-bearing flanking fades in the Middle Missis-
sippian of the Illinois Basin: American Association of Petroleum Geologists,
1994 Abstract Volume.

Lasemi, Z., J.D. Treworgy, and R.D. Norby, 1994b, Depositional history of
the Mississippian Ullin and Fort Payne Formations in the Illinois Basin:
Geological Society of America, 1994 Abstract Volume.

Lees, A., 1961 , The Waulsortian "reefs" of Eire: A carbonate mudbank complex
of Lower Carboniferous age: Journal of Geology, v. 69, p. 101-109.

Lees, A., 1988, Waulsortian "reefs": The history of a concept: Mem. Inst,
geol. Univ. Louvain, 34, p. 43-55.

Lees, A., and J. Miller, 1985, Fades variation in Waulsortian buildups, Part 2:
Mid-Dinantian buildups from Europe and North America: Geological Journal,
v. 20, p. 159-180.

Lineback, J.A., 1966, Deep-Water Sediments Adjacent to the Borden Siltstone
(Mississippian) Delta in Southern Illinois: Illinois State Geological Survey,
Circular401,48p.

Lineback, J.A., 1969, Illinois Basin — sediment-starved during the Mississippian:
American Association of Petroleum Geologists Bulletin, v. 53, no. 1 ,
p. 112-126.

Lineback, J.A., 1981, The Eastern Margin of the Burlington-Keokuk (Valmey-
eran) Carbonate Bank in Illinois: Illinois State Geological Survey, Circular
520, 24 p.

Lineback, J.A., and R.M. Cluff, 1985, Ullin-Fort Payne, A Mississippian shallow
to deep water carbonate transition in a cratonic basin, in P.D. Crevello, and
P.M. Harris (eds.), Deep-Water Carbonates: Buildups, Turbidites, Debris

Flows and Chalks: Society of Economic Paleontologists and Mineralogists
Core Workshop 6, p. 1-26.

MacQuown, W.C., and J.H. Perkins, 1982, Stratigraphy and petrology of
petroleum producing Waulsortian-type carbonate mounds in Fort Payne
Formation (Lower Mississippian) of north central Tennessee: American
Association of Petroleum Geologists Bulletin, v. 66, p. 1055-1075.

Miller, J., and R.F. Grayson, 1982, The regional context of Waulsortian fades
in northern England , in K. Bolton, H.R. Lane, and D.V. LeMone (eds.),
Symposium on the Paleoenvironmental Setting and Distribution of the
Waulsortian Facies: El Paso Geological Society and the University of
Texas at El Paso, p. 17-33.

Monty, C.L.V., M.C. Bemet-Rollande, and A.F. Maurin, 1982, Re-interpretation
of the Frasnian classical "reefs" of the southern Ardennes, Belgium: Ann.
Soc. geol. Belgique, v. 105, p. 339-341.

Morgan, G.R., and D.E. Jackson, 1970, A probable "Waulsortian" carbonate
mound in the Mississippian of northern Alberta: Bulletin of Canadian Petro-
leum Geology, v. 18, p. 104-112.

Philcox, M.E., 1967, A Waulsortian bryozoan reef ("cumulative biostrome")
and its off-reef equivalents, Ballybeg, Ireland: Compte Rendu, Sixth
International Congress of Stratigraphy and Geology of the Carboniferous,
Sheffield, England, v. 4, p. 1359-1372.

Pratt, B.R., 1982, Stromatolitic framework of carbonate mud-mounds: Journal
of Sedimentary Petrology, v. 52, p. 1203-1227.

Pray, L.C., 1958, Fenestrate bryozoan core facies, Mississippian bioherms,
southwestern United States: Journal of Sedimentary Petrology, v. 28,
p. 261-273.

Precht, W.F., and W. Shepard, 1989, The structure, sedimentology and
diagenesis of some Waulsortian carbonate buildups of Mississippian age
from Montana, in H.H.J. Geldsetzer, N.P. James, and G.E. Tebbutt (eds.),
Reefs, Canada and Adjacent Areas: Canadian Society of Petroleum
Geologists, Memoir 13, p. 682-687.

Sevastopulo, G.D., 1982, The age and depositional setting of Waulsortian
limestones in Ireland, in K. Bolton, H.R. Lane, and D.V. LeMone (eds.),
Symposium on the Paleoenvironmental Setting and Distribution of the
Waulsortian Facies: El Paso Geological Society and the University of
Texas at El Paso, p. 65-79.

Smith, D.L., 1977, Transition from deep- to shallow-water carbonates, Paine
Member, Lodgepole Formation, central Montana, in H.E. Cook, and
P. Enos (eds.), Deep-Water Carbonate Environments: Society of Economic
Paleontologists and Mineralogists, Special Publication 25, p. 187-201.

Treworgy, J.D., ST. Whitaker, and Z. Lasemi, in review, 1 1 :30 O'Clock
Cross Section in the Illinois Basin, Wayne County to Stephenson County,
Illinois: Illinois State Geological Survey, Open File Series.

Treworgy, J.D., M.L. Sargent, and D.R. Kolata, 1991, Tectonic subsidence
history of the Illinois Basin (extended abstract), in Program with Abstracts
for the Louis Unfer, Jr., Conference on the Geology of the Mid-Mississippi
Valley, Cape Girardeau, MO, 6 p.

Tsien, H.H., 1985, Algal-bacterial origin of micrites in mud mounds, in
D.F. Toomey, and M.H. Nitecki (eds.), Paleoalgology: Contemporary
Research and Applications: Springer-Verlag, Berlin, p. 290-296.

West, R.R., 1988, Temporal changes in Carboniferous reef mound communi-
ties: Palaios, v. 3, p. 152-169.

Wilson, J.L., 1969, Microfacies and sedimentary structures in "deeper water"
lime mudstones, in G.R. Friedman (ed.), Depositional Environments in
Carbonate Rocks (symposium): Society of Economic Paleontologists and
Mineralogists, Special Publication 14, p. 4-19.

Wilson, J.L, 1975, Carbonate Fades in Geologic History: Springer-Verlag,
New York, 471 p., esp. p. 165-167 and chapter V.

Wright, V.P., and T.J. Faulkner, 1990, Sediment dynamics of Early Carbonif-
erous ramps: A proposal: Geological Journal, v. 25, p. 139-144.

PETROLEUM OCCURRENCE IN THE ULLIN
LIMESTONE ("WARSAW")

John P. Grube

The thinly scattered petroleum reservoirs in the Ullin Limestone ("Warsaw")
in the Illinois Basin (fig. 40) were rarely prolific prior to the 1990s. There are
69 fields with reported "Warsaw" production in Illinois, but only 13 fields list
ten or more wells that have produced from the "Warsaw," and 37 fields have
three or fewer wells that have produced "Warsaw" oil (appendix). "Warsaw"
production accounts for approximately 1% of the more than 4 billion barrels
of oil recovered from Illinois Basin reservoirs.

The basin is undergoing a third round of Ullin ("Warsaw") development.
There have been two previous periods of development of "Warsaw" fields: one
during the late 1 950s and early 1960s when the pay was initially discovered,
and the second during the drilling boom of the late 1970s and early 1980s.
In the early 1 990s, the completion of prolific wells in two fields, Johnsonville
Consolidated in Wayne County and Enfield South in White County, once again
heightened interest and promoted drilling in the "Warsaw" pay. Completions
of flowing wells of 200 to 400 barrels of oil per day are not uncommon. These
wells continue to have high rates of production. Records indicate that some
wells have produced in excess of 100,000 barrels of oil in less than 2 years.

Two of the better fields discovered during the earlier exploratory phases are
Bessie and Ewing East, both located in Franklin County, Illinois. Each field has
produced approximately 1 .5 million barrels of oil. Wells in Bessie Field, dis-
covered in 1979, have average estimated reserves of 90,000 barrels of oil
per well (Strothmann 1988). Several wells in this field have cumulative production
exceeding 250,000 barrels of oil and are presently pumping about 20 barrels
per day (appendix). Ewing East wells have lower reserves; however, at
least 12 wells have cumulative production greater than 50,000 barrels of oil per
well. Depth to the producing intervals in these two fields is approximately
3,800 to 4,000 feet. Depth to the "Warsaw" pay throughout Illinois ranges from
2,400 feet on the La Salle Anticlinorium to 4,400 feet in the heart of the Fair-
field Basin (Wayne, White, and Hamilton Counties).

Hydrocarbon reservoirs in the Ullin ("Warsaw") are found in thin, discontinuous,
porous lenses that commonly develop in the upper 100 feet of Ullin-type rock.
A porosity log (fig. 41) from the Porter-Weaver Community no. 1 , Section 8,
T1S, R6E, one of the better "Warsaw" producers in Johnsonville Consolidated,
shows the development of excellent porosity in the uppermost part of the
Ullin ("Warsaw"). The hydrocarbon charge exists only in the intervals from
3,974 to 3,980 feet and 3,983 to 3,986 feet. The lower porosity zones are wet,
typical of "Warsaw" production. Locally in Johnsonville, Enfield South and the
Franklin County fields, the porosity equivalent to that below 3,998 feet in the
Porter-Weaver Community no. 1 is commonly wet, even where the upper
porosity is absent. The Porter-Weaver Community no. 1 has produced more
than 240,000 barrels of oil in 22 months.

Core from the Ullin ("Warsaw") is scarce, and therefore measured values for
porosity and permeability are hard to obtain. Porosity logs indicate that aver-
age porosity for reservoir rock ranges from 8% to 10%. As the experiences of
oil field operators and porosity log examination show, wells with less than 6%
porosity are nonproductive, probably because of low permeability.

Hydrocarbon reservoirs are generally found in porous zones commonly less
than 10 feet thick in the upper 100 feet of the "Warsaw." The most productive

Figure 40 Distribution of Ullin/Harrodsburg/"Warsaw" hydrocarbon production in the Illinois Basin (from Howard 1991).

BOOTH OIL CO., INC.

Porter-Weaver Comm. no. 1

T1S-R6E-Sec8NESESE

Wayne Co., IL

Gamma

Micro-
Resistivity

10%

Figure 41 Porosity log of the Porter-Weaver Community no. 1 , Sec. 8-T1 S-
R6E, one of the better Ullin ("Warsaw") producers in Johnsonville
Consolidated. Note development of excellent porosity in the uppermost
part of the unit. The hydrocarbon charge exists only from 3974-80 feet and
from 3983-86 feet. The lower porosity zones are wet.

wells are associated with the development of multiple, porous zones, particu-
larly in the uppermost part of the "Warsaw" (fig. 41). In these wells, only the
top one or two porous zones produce hydrocarbons; the underlying porous
zones produce only water.

A review of the Ullin ("Warsaw") fields in Illinois shows that a combination of
structure and stratigraphy define the play. The critical components for the
trapping of hydrocarbons are development of effective porosity and draping
of the porous interval across a structure. Structural closure on the reservoir is
not critical. Isopach mapping and trend projections based on geometric analy-
sis of specific porosity development are fundamental to the discovery and de-
velopment of "Warsaw" fields.

Thickness of the total Ullin ("Warsaw") (fig. 35) defines the boundary of the
play within the basin. At present, most production is confined to that part of
the basin where the thickness of the "Warsaw" exceeds 200 feet. The only
production found where the Ullin ("Warsaw") is less than 200 feet thick is in
the area that borders the west side of the Wabash River (figs. 35, 40). Fur-
ther evaluation of porosity development and hydrocarbon migration may ex-
pand the boundary of the Ullin ("Warsaw") play.

REFERENCES

Howard, R.H., 1991, Hydrocarbon reservoir distribution in the Illinois Ba-
sin, in M.W. Leighton, D.R. Kolata, D.F. Oltz, and J.J. Eidel (eds.), Interior
Cratonic Basins: American Association of Petroleum Geologists, Memoir 51 ,
p. 299-327.

Strothmann, K., 1988, Bessie Field, in C.W. Zuppann, and B.D. Keith (eds.),
Geology and Petroleum Production of the Illinois Basin: Illinois and Indiana-
Kentucky Geological Societies, v. 2, p. 103-104.

VULCAN MATERIALS COMPANY REED
QUARRY, LIVINGSTON COUNTY, KENTUCKY

Garland R. Dever, Jr.
Kentucky Geological Survey

Terry Teitloff
Vulcan Materials Company Reed Quarry

The top producer of crushed stone in the United States during recent years
has been the Reed quarry in Livingston County, Kentucky. In 1992, its produc-
tion was 10.27 million tons (Prokopy 1993).

Opened in 1950 by the Clyde Reed Trucking Company, the quarry was oper-
ated for many years by the Reed Crushed Stone Company. Vulcan Materials
Company purchased the operation in 1990.

Crushed stone has been produced from three Mississippian formations (in
descending order), the Salem Limestone, Warsaw Limestone (Kentucky
terminology), and Fort Payne Formation.

The Salem is composed of (1) olive to medium gray, fine to very coarse
grained, bioclastic limestone that is locally cherty, and (2) olive gray to olive
black, very finely crystalline limestone that is partly argillaceous to shaly and
locally cherty.

The principal lithology of the Warsaw is very light to medium gray, fine to very
coarse grained, bryozoan and crinoidal limestone. The Warsaw, particularly
in the lower part, contains lenses and beds of olive gray to grayish black,
micrograined to fine grained limestone and fine to coarse grained bioclastic
limestone, both of which are commonly argillaceous and cherty.

The Fort Payne mainly is composed of medium dark to dark gray, very fine to
fine grained, siliceous limestone. The silica content of the Fort Payne varies,
but averages about 20%.

The quarry face is divided into eight ledges, which furnish a frame of reference
for describing the quarry. Ledge 1 at the top of the pit and part of underlying
ledge 2 are in the Salem. The Warsaw encompasses part of ledge 2, ledges
3 and 4, and the uppermost part of ledge 5. Most of ledge 5 and ledges 6, 7,
and 8 are in the Fort Payne. The average height of ledges 2, 3, and 4 is about
60 feet. Each Fort Payne ledge, 5 through 8, is about 70 feet high. Ledge 1 ,
along the lip of the quarry, varies in height.

In recent years, there has been no production from ledge 1 and very little
from ledge 2, mainly riprap. Bryozoan-crinoidal limestone of the Warsaw in
ledges 3 and 4 was the quarry's principal source of construction and agricultural
stone for a number of years. Because they have the highest calcium carbonate
content of all ledges in the present quarry, ledges 3 and 4 are now reserved for
markets requiring chemically pure stone. From 1984 to 1989, limestone of
ledge 3 was used in a flue-gas desulfurization, wet-scrubbing system at the

Big Rivers Electric Corporation, Wilson power plant in Ohio County, Kentucky.
It was also used as sorbent stone in a 20-megawatt atmospheric fluidized-bed
combustion pilot plant located near Paducah, Kentucky, and operated by the
Tennessee Valley Authority. Ledge 4 currently is the quarry's main source for
agricultural limestone.

In the early 1980s, the quarry was deepened to open up the Fort Payne for
production. Siliceous limestone of the Fort Payne is being used for railroad
ballast, bituminous and concrete aggregate, skid-resistant aggregate (Louisiana
and Kentucky only), bank-paving material (riprap), and filter beds (both for
sewage treatment and scrubber-sludge dewatering).

The Reed quarry ships about 75% of its production by barge, 15% by rail, and
10% by truck. The Gulf Coast region is the destination for most of the stone,
mainly riprap and aggregate, that is transported by barge.

REFERENCE

Prokopy, S., 1993, Top 20 crushed stone plants: Rock Products, v. 96, no. 10,
p. 55-58.

INDUSTRIAL USES OF THE ULLIN
LIMESTONE ("WARSAW")

Richard D. Harvey

The Harrodsburg Member (upper part of the Ullin Limestone) has distinctive
qualities that make it valuable for the two main uses of crushed stone, agricul-
tural limestone (to neutralize the acidity and improve the texture of soils) and
construction aggregates. At the Jonesboro quarry (Stop 3), the limestone
generally tests greater than 96% CaC03, approximately 3% to 4.5% water
absorption, and almost 2.4 g/cc bulk density. These data indicate an average
porosity of about 11%. Such qualities of purity and implied softness make this
stone exceptionally valuable as an agricultural limestone, which represents
about 40% of the production at this quarry.

Although tests by the Illinois Department of Highways of various gradations
of the crushed stone confirm the quarry products to be too soft (average
abrasion loss is 43%) and skid resistance too low for use as aggregates in
Portland cement concrete pavements, the tests do qualify this stone to be used
for other road and construction materials where specifications of abrasion are
less stringent. About 10% of the production from this quarry is sold for road-
base materials and the coarse aggregates used on county roads.

From a nearby quarry, the Harrodsburg was used during the 1960s and early
1970s as dimension stone. At that quarry, the limestone is uniformly thick
bedded, which allowed it to be quarried into big blocks and slabbed. The
slabs were easily fabricated into a variety of building uses. The stone takes
an excellent polish for special decorative veneers. Several buildings in
nearby towns, especially Anna and Jonesboro, are veneered with this stone.

Since about 1970, a new market for limestones and dolomites developed,
using their calcined product (lime or magnesia derived from a heating process)
as an absorbent of sulfur oxides from flue gases that are generated by com-
bustion of coal. Studies have shown that the Harrodsburg is uniquely suited
for certain desulfurization processes, mainly those classified as wet-limestone
"scrubbing" (Harvey et al. 1 974) and, to a lesser extent, fluidized-bed combustion
(Rostam-Abadi et al. 1989). The Harrodsburg, as quarried at Jonesboro,
provided the highest SO2 reactivity of the 1 1 rather typical carbonate rocks that
were laboratory tested. Microscopic analyses suggest that the high reactivity
of this stone is due to the high porosity that exists between the 5 to 20 |im calcite
crystallites that constitute the abundant bryozoan fragments. Another con-
tributing factor may be traces of highly reactive soluble salts (mainly NaCI) that
occur as fluid inclusions within the large crystals that constitute the crinoid frag-
ments. The light gray chert that occurs as a minor constituent in several beds of
the Harrodsburg has the negative effect of diluting the abundance of the reactive
calcite and causes extra wear on crushing and grinding equipment. Currently
about 50% of the production from the Jonesboro quarry is used for desulfuri-
zation purposes in scrubbers at two power plants, one in Sikeston, Missouri,
and the other (Southern Illinois Power Cooperative) in Marion, Illinois.

In the study by Rostam-Abadi et al. (1989), thermal gravimetric analyses of
the 300 to 425 \im particles from this quarry absorbed more SO2 than all other
limestones tested. However, for the same study, in tests designed to simulate
desulfurization under pressurized fluidized-bed combustion, this stone did not
perform as well as many dolomites. The high reactivity of dolomites in the
fluidized-bed environment is thought to be aided by the high porosity that is
developed within the calcined products from dolomites. A considerable pro-
portion of the calcium oxide that is produced during heating of dolomites is
thought to form as ultrafine grains on the surfaces of the calcine, thus making
the calcium readily available and exceptionally reactive with SO2. To date,
the market for other midwestern limestones for desulfurization have not signifi-
cantly increased. The importation of low-sulfur coal (subbituminous) into
midwestern power-generating plants has steadily increased during the past
few years, and this trend is not expected to change in the near future. Substi-
tution of fuels other than coal has limited the market for desulfurization with
carbonate rocks.

REFERENCES

Harvey, R.D., R.R. Frost, and J. Thomas, Jr., 1974, Lake marls, chalks, and
other carbonate rocks with high dissolution rates in SO2 - scrubbing
liquors, in Tenth Forum on Geology of Industrial Minerals: Ohio Geological
Division Miscellaneous Report 1, p. 67-80; also Illinois State Geological
Survey, Environmental Geology Notes 68.

Rostam-Abadi, M., W.-T. Chen, R.D. Harvey, and MP. Cal, 1989, Sorbent
evaluation for pressurized fluidized-bed combustors: Illinois State Geological
Survey, Final Technical Report, 56 p.

Appendix Production history to January 1994 for Ullin ("Warsaw") fields (Source: B.G. Huff)

Field

Discovery well
Company

Farm name and number

Total

depth Completion

(ft) date

Aden Consolidated

H.H. Weinert

Morlan "B" No. 5

Akin West

Texaco

U.S. Steel No. 1

Albion Consolidated

Superior Oil Company

J.C. Blood No. A-10

Allendale

Bridgeport Drilling

M. Pace No. 1

Bamhill

Ivan R. Jones

Zurliene No. 1

Belle Prarie West

Calvert Drilling

Rawls No. 1

Belle Rive

C. E. Brehm

Foster Community N

Benton

Shell Oil Co.

C W & F Coal No. 1

Benton North Great Plains Resources Old Ben No. 2-H

Berryville Consolidated Southern Triangle H. Pixley No. 1

Bessie

Blairsville West
Consolidated

Broughton

Browns

C. E. Brehm Drilling &
Producing

J.D. Turner

Duke Resources
Tartan Oil

Summers-U.S. Steel No. 1

F.C. Morris & Sons No. B-1

Bonan No. 1

A.J. Messman No. 2-A

4148

3900

6/9/59

5185

4/19/62

4511

9/19/80

2864

10/21/66

4378

9/20/81

4389

5/5/59

4100

2/10/79

6250

3/16/60

3656

11/10/83

3688

1/21/75

11/27/79

4565 2/17/81

4269 11/11/77

3825 2/14/84

Bungay Consolidated E.D. Dupont, Jr.

S.L. Moore No. 1-B

Calhoun East Bunn & Bunn Oil Co., Inc. B. Williams No. 1

Centerville Jim Haley Oil Production Martin R. Barbre No. 2

Clay City Consolidated Pure Oil Company E. Walters No. 2

4290

12/22/59

4166 7/9/85

4140 10/15/82

3646 12/23/52

Concord Consoldiated

Jim Haley Oil Production

W.R. Tuley No. 6

3965

3/1/75

Covington South

Peake Petroleum
Company

Feathers et al. No. 1

4148

9/7/60

Crossville West

The French Creek Co.

George Spencer No. 2

4207

2/25/83

Dahlgren

Athene Development

C.L Serivener No. 1

5299

11/27/56

Dahlgren South

Homco Ltd.

Koberlein No. 1

4366

9/24/82

Dahlgren Southwest

Ashland Exploration

Lena Cross No. 1

4585

8/2/83

Dahlgren West

Sun Oil Company

R.W. Aydt No. 1

5245

11/16/60

Discovery

well

(Sec-T-R)

County

Initial

production

BO/BW/DAY*

Depth to
"Warsaw"
zone (ft)

Thickness
of zone
(apprx ft)

No. of

"Warsaw"

wells

Comments

33-2S-7E

Wayne

138 BO

4132

First reported Warsaw
production in state, also
deepest pay at time

20-6S-4E

Franklin

82 BO

3994

1-3S-10E

Edwards

40 BO/130 BW

3978

I. P. includes production
from Salem

33-2N-12W

Wabash

50 BO/50 BW

2806

9-3S-8E

Wayne

30 BO/20 BW

4214

Dry hole drilled deeper,
OTD 3602; LP. includes
Salem and Rosiclare

1-4S-5E

Hamilton

24 BO/70 BW

4206

22-3S-4E

Jefferson

9 BO/75 BW

3985

Old well drilled deeper

36-6S-2E

Franklin

261 BO/160 BW

3705

I. P. from 5 zones
including McClosky and
St. Louis discoveries

12-6S-2E

Franklin

60 BO/15 BW

3656

31-2N-13W

Wabash

7 BO/10 BW

3605

LP. includes production
from Salem discovery

13-6S-3E

Franklin

150 BO

3825

13-4S-6E

Hamilton

20 BO

4336

LP. includes production
from Salem discovery

27-6S-7E

Hamilton

580 BO

4191

33-1S-14W

Wabash

33 BO/70 BW

3810

Old well drilled deeper;
was Cypress and
McClosky producer

10-4S-7E

Hamilton

14 BO/100 BW

4190

LP. includes production
from McClosky

6-2N-11E

Richland

18 BO/8 BW

4099

12-4S-9E

White

91 BO/80 BW

4120

Extension to field

5-3N-9E

Richland

54 BO/96 BW

3600

LP. includes production
from McClosky, St. Louis
and Salem

21-6S-10E

White

20 BO

3868

14-2S-6E

Wayne

175 BO

4136

22-4S-10E

White

20 BO/10 BW

4128

LP. includes production
from Aux Vases

27-3S-5E

Hamilton

1 1 BO/90 BW

4110

30-4S-5E

Hamilton

75 BO/20 BW

4275

15-4S-4E

Jefferson

3 BO/14 BW

4216

1-4S-4E

Jefferson

150 BO/100 BW

4019

Old well worked over;
abandoned 1966

Appendix continued

Field

Discovery well
Company

Farm name and number

Total
depth
(ft)

Completion
date

Dale Consolidated

Ernest Sherman

W.E. Hunt et al. Unit No. 1

4180

4/25/78

Deering City

The Wiser Oil Company

Peabody Coal Co. No. 1

3748

12/10/85

Divide Consolidated

William & Phyllis Becker

Mammie Floweree No. 2

3601

8/4/81

Ellery East

Sandy Ridge Oil Co., Inc.

Harold Perkins No. 1

4227

1 1/25/78

Ellery South

Modern Exploration

Glover No. 1

4159

12/4/78

Enfield

Pricefields Oil, Inc.

Fields-West No. 1

4358

8/1/77

Enfield North

R.K. Petroleum

Triple AAA Ranch No. 4

4392

5/17/77

Enfield South

Wilbanks Exploration

Warren No. 1-6

4294

11/1/90

Ewing

Geo. Mitchell Drilling

Dalby No. 1

3821

4/25/81

Ewing East

C.E. Brehm

Clayton Heirs Comm. No. 1

9511

10/12/76

Flora South

Dart Oil & Gas

Levitt-McHenry Comm. No.
5-1

4900

4/22/82

Gards Point
Consolidated

Louis A. Pessina

J.A. Fishel No. 1

3705

8/19/75

Goldengate
Consolidated

T.G. Jenkins

T.G. Jenkins No. 1

4135

1 1/8/61

Goldengate North
Consolidated

Humboldt Oil Company

E. Webb No. 1

4750

4/17/84

Herald Consolidated

C.E. Brehm Drilling &
Production

Rupp No. 1

5285

5/29/76

Johnsonville
Consolidated

Mid-American Petroleum

Dickey No. 2

3938

10/31/80

Johnsonville West

Joe A. Dull

Cravens No. 1

3824

8/30/78

Lawrence

Hubert Rose

Ackman No. 1

3387

5/10/83

Louisville

Texaco

John Paul Kincaid No. 1

4865

11/2/74

Macedonia

C.E. Brehm Drilling &
Production

Hutchcraft Unit No. 1

5249

2/15/61

Maple Grove
Consolidated

Energy Resources

P.M. Weber No. 5

4057

8/10/76

Maple Grove South
Consolidated

Maunie North
Consolidated

Collin Bros.

Grover Hines No. 1

6119

4/15/80

Maunie South
Consolidated

Rhea Fletcher

Flora Karch No. 3

4256

7/29/74

Mayberry

Commanche Oil Corp.

Parker Comm. No. 1

5373

1/14/77

Mayberry North

E.S. Guilliams

Legg & Bryant

4311

10/2/81

Mayberry South

V.R. Gallagher

Trotter No. 1

4350

8/19/81

Discovery Initial Depth to Thickness No. of

well production "Warsaw" of zone "Warsaw"

(Sec-T-R) County BO/BW/DAY* zone (ft) (apprx ft) wells

Comments

21-6S-7E

Hamilton

20 BO

4124

16-7S-3E

Franklin

20 BO

3748

21-1 S-4E

Jefferson

7 BO/10 BW

3502

3-3S-10E

Edwards

16 BO/18 BW

4218

4-3S-10E

Edwards

125 BO

4156

17-5S-8E

White

10 BO

4318

9-5S-8E

White

50 BO

4385

6-6S-8E

White

40 BO/100 BW

4294

3-5S-3E

Franklin

4 BO/75 BW

3790

2-5S-3E

Franklin

104 BO/70 BW

3880

5-2N^6E

Clay

125 BO

3707

14-1N-14W

Wabash

14 BO

3698

29-2S-9E

Wayne

40 BO

4125

5-2S-9E

2-7S-9E

20-1 S-6E

35-1 N-5E
6-2N-11W
28-4N-6E

24-5S-4E

Wayne 45 BO

White

Wayne

Lawrence

Clay

Franklin 75 BO

4323

25 BO/30 BW

3961

15 BO/30 BW

3823

14 BO/12 BW

3823

45 BO/100 BW

2420

107 BO/60 BW

3534

22-1 N-9E Wayne 25 BO/30 BW

4097

4050

6
9

1
2

1
5
1
6

40
1

1
33

1
1
2

Extension to field

I. P. includes production
from Ohara

Also field extension

Extension to field

IP. includes production
from St. Louis

Old well drilled deeper;
was D&A, old TD 3102

Old well worked over

Discovery well of field; LP.
includes Aux Vases,
McClosky & Salem

Dry and abandoned well
worked over

2-6S-10E

White

oil well

24-6S-10E

White

51 BO/240 BW

3964

8-3S-6E

Wayne

200 BO/20 BW

4297

27-2S-6E

Wayne

40 BO/70 BW

4194

16-3S-6E

Wayne

47 BO/28 BW

4282

See Samsville West for
Warsaw Discovery

LP. not reported.
Produces from Salem also

LP. includes production
from St. Louis

Appendix continued

Field

Discovery well
Company

Farm name and number

Total

depth Completion

(ft) date

Mill Shoals
Mt. Carmel

Nation Oil W. P. Mcintosh No. 2 4191 11/4/59

Farmers Petroleum Co-op Wabash-Newton No. 3 3117 11/1/77

New Harmony
Consolidated

Noble West

Hubert Rose

Vida King No. 1

3712

10/29/79

Norris City West

Olney South

Parkersburg
Consolidated

Phillipstown
Consolidated

Reynolds & Vincent

Mary Britton Comm. No. 1

Frank Yockey and Yockey Walter Schonert No. 2
Oil, Inc.

Viking Oil Co.

Louis Pessina

Roland Consolidated Southern Triangle

Rural Hill North

Juniper Petroleum Inc.

Imogene Fishel No. 1

E.H. Morris "A" No. 1

H. Ward No. 1

Clark-Meneghin 47-34

4460

4/18/78

3935

9/12/90

4118

6/28/78

4100

2/12/80

4123

1/11/66

4275

3/15/77

Samsville West

Spartan Petroleum

Leonard Garman No. 2

4175 5/31/77

Springerton South
Storms Consolidated

Sumpter North
Taylor Hill
Walpole
Whittington

Perry Fulk Hazelip No. 1

Atek Drilling & Production L. Cutchin No. 1

Absher Oil C. Bohleber No. 1

Leo Horton Webb Heirs No. 1

Henry Energy Corporation Johnson Heirs No. 1

H & W Oil Company Adams No. 1

4385

6/18/77

4038

12/16/84

4335

8/3/74

3970

1/18/61

5950

6/20/85

3719

2/21/77

'Barrels of oil, barrels of water per day

Discovery

well
(Sec-T-R)

County

Initial

production

BO/BW/DAY*

Depth to
"Warsaw"
zone (ft)

Thickness
of zone
(apprx ft)

No. of

"Warsaw"

wells

Comments

31-3S-8E
8-1S-12W

White
Wabash

57 BO/110 BW
20 BO/30 BW

4110
3097

10
10

7
5

Old well drilled deeper,
formerly D & A

3755

Discovery well unknown

3-3N-8E

30-6S-8E

17-3N-10E

Clay

21 BO/210 BW 3695

White 38 BO

4204

Richland 10 BO/30 BW 3894

IP. includes production
from Salem and
McClosky; also field
extension

Dry hole drilled deeper;
also discovery of Norris
City West field

17-2N-14W Richland 20 BO/30 BW

30-3S-11E White

36-5S-8E

White

8 BO

25 BO

34-5S-5E Hamilton 89 BO/64 BW

3966

3990

4050

4220

3
23

19
6

IP. includes production
from Salem

IP. includes production
from Ohara and St. Louis
discoveries

22-1N-10E

Edwards

20 BO/40 BW

4170

Incorporated into Maple
Grove South Consolidated
1977

28-4S-8E

White

15 BO/100 BW

4379

11-6S-9E

White

49 BO

4030

IP. includes production
from Spar Mountain and
St. Louis

21-4S-9E

White

10 BO/30 BW

4230

16-5S-4E

Franklin

8 BO

3940

Old well worked over

27-6S-6E

Hamilton

60 BO

4194

30-5S-3E

Franklin

20 BO

3562

D & A well drilled deeper,
IP. includes production
from Salem discovery

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