Louisiana State University LSU Digital Commons LSU Historical Dissertations and eses Graduate School 1966 Aspects of Early Allegheny Depositional Environments in Eastern Ohio. Ronald K . Zimmerman Louisiana State University and Agricultural & Mechanical College Follow this and additional works at: hps://digitalcommons.lsu.edu/gradschool_disstheses is Dissertation is brought to you for free and open access by the Graduate School at LSU Digital Commons. It has been accepted for inclusion in LSU Historical Dissertations and eses by an authorized administrator of LSU Digital Commons. For more information, please contact [email protected]. Recommended Citation Zimmerman, Ronald K., "Aspects of Early Allegheny Depositional Environments in Eastern Ohio." (1966). LSU Historical Dissertations and eses. 1175. hps://digitalcommons.lsu.edu/gradschool_disstheses/1175
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Louisiana State UniversityLSU Digital Commons
LSU Historical Dissertations and Theses Graduate School
1966
Aspects of Early Allegheny DepositionalEnvironments in Eastern Ohio.Ronald K. ZimmermanLouisiana State University and Agricultural & Mechanical College
Follow this and additional works at: https://digitalcommons.lsu.edu/gradschool_disstheses
This Dissertation is brought to you for free and open access by the Graduate School at LSU Digital Commons. It has been accepted for inclusion inLSU Historical Dissertations and Theses by an authorized administrator of LSU Digital Commons. For more information, please [email protected].
Recommended CitationZimmerman, Ronald K., "Aspects of Early Allegheny Depositional Environments in Eastern Ohio." (1966). LSU HistoricalDissertations and Theses. 1175.https://digitalcommons.lsu.edu/gradschool_disstheses/1175
This dissertation has been microfilmed exactly as received 6 6 -1 0 ,9 2 5
ZIM M ERM AN, R onald K „ 1 9 3 5 - A S P E C T S O F E A R L Y A L L E G H E N Y D EPO SITIO N A L EN V IR O N M EN TS IN E A S T E R N OHIO.
L o u is ia n a State U n iv e r s ity , P h .D ., 1966 G eo lo g y
University Microfilms, Inc., Ann Arbor, Michigan
ASPECTS OF EARLY ALLEGHENY DEPOSITIONAL ENVIRONMENTSIN EASTERN OHIO
A Dissertation
Submitted to the Graduate Faculty of the Louisiana State University and
Agricultural and Mechanical College in partial fulfillment of the requirements for the degree of
Doctor of Philosophyin
The Department of Geology
byRonald K. Zimmerman
B.S., University of Illinois, 1960 M.S., Louisiana State University, 196 3
May, 1966
ACKNOWLEDGMENT S
The writer wishes to express his gratitude to the
various members of the faculty who reviewed the manuscript. Particular notes of gratitude are due Dr. John C. Ferm,
Associate Professor of Geology/ for introducing the author to the problem, critically guiding the study to completion and providing funds for field study under NSF grant G-18816
Dr. J. Keith Rigby, Visiting Professor of Geology (1964-65),
for assisting with identification of fossils in the carbonates; Dr. Frank Iddings, of the LSU Nuclear Science Center,
for assisting with the neutron activation analyses of the ironstones; Mr. Lewis G. Nicols, for assistance with photomicrographs; Mr. Philip B. Larimore, for assistance in
drafting the illustrations; the Ohio Geological Survey for making available unpublished descriptions of stratigraphic sections; and to numerous persons in the field area for
permitting access to their property. Notes of appreciation are also expressed to fellow graduate students; Romeo M.
Flores, Victor V. Cavaroc, Jr., and Harry H. Roberts, all of whom have completed or are' presently engaged in work on
ii
the Allegheny rocks, for the many critical discussions and arguments concerning the study; and John B. Echols and others, too numerous to mention, who acted as sounding boards for my ideas concerning the study.
Finally, I owe a special expression of gratitude to my wife, Mary Lou Camp Zimmerman, and family for their encouragement and forbearance during the course of this study.
TABLE OP CONTENTS
Page
ACKNOWLEDGMENTS i iLIST OF PLATES, FIGURES, AND TABLES....................... vii
ABSTRACT.................................................. X
Petrographic Summary and Paleogeographic Inferences.................................. 46
IV. RECONSTRUCTION OF DEPOSITIONALENVIRONMENTS.................................... 49
Introduction.................................. 49Sedimentary Development of the LowerAllegheny ......................... 54
V. SUMMARY AND CONCLUSIONS............... 66
v
PageREFERENCES C I T E D ........................ 69A P P E N D I X ...................................... 73
V I T A .......................................... 123
vi
LIST OF PLATES
Plate Page
I. Location of stratigraphic control" . . . in envelope
II. Cross section A - B .........................in envelopeIII. Cross section C - D .............. in envelopeIV. Cross section E-F & G - J in envelope
V. Cross section I-J-H & K - H - M .............. in envelopeVI. Cross section C-L . .................... in envelope
LIST OF FIGURES Figure Page
1. Allegheny outcrop area on flanks ofAllegheny Synclinorium. . . . . .............. 3
2. Schematic cross section of lower Alleghenyrocks in eastern O h i o ......................... 7
3. Outcrop of the Clarion Formation in northeastern Ohio .............................. 8
4. Depositional models applicable to thegenesis of lower Allegheny rocks.............. 21
5. Index map of 15 minute quadrangles showing chemical rock sampling localities . .......... 23
6 . Ironstones in the upper Clarion at the Newcastle no. 2 s e c t i o n ........... ........... 25
vii
Figure Page7. Schematic cross section of lower Allegheny
marine-brackish-freshwater zones ineastern Ohio.............................. 29
8 . Photomicrograph of section 2397 .............. 379. Photomicrograph of section 2 4 1 4 .............. 37
10. Photomicrograph of section 2403 .............. 38
11. Photomicrograph of section 2 4 1 5 .............. 3812. Photomicrograph of section 2 4 1 1 .............. 3913. Photomicrograph of section 2 4 1 6 ........... . 39
14. Photomicrograph of section 2393 .............. 4015. Photomicrograph of section 2399 .............. 4016. Schematic cross section showing major
phases of progradation in eastern Ohio. . . . 50
17. Early Allegheny paleogeography;phases 1 & 2.............................. 52
18. Early Allegheny paleogeography? phase 2A. . . 5519. Early Allegheny paleogeography; phase 3 . . . 5820. Early Allegheny paleogeography; phase 4 . . . 6121. Early Allegheny paleogeography; phase 5 . . . 63
LIST OF TABLES
Table Page
I. Silicon content in ironstone concretions. . . 26II. Index to limestone samples. . ............. 31
IV. Limestone thin section point countestimates............... 35
ix
ABSTRACT
Lower Allegheny rocks of Middle Pennsylvanian age in eastern Ohio comprise a variety of chemical and detrital
rock types each presumably reflecting a particular environment of deposition. Temporally and spatially these environments had a complex albeit systematic chronological arrangement, the reconstruction of which was achieved by
collecting, analyzing, and integrating the data from both field study of the spatial relationships of rock types and
detailed study of some of the chemical components (iron
stones and limestones). Results from these lines of evi
dence were interpreted in light of information from similar studies in southern Ohio and western Pennyslvania. Deposition of the lower Allegheny rocks was apparently in and around a complex set of prograding deltaic wedges. The direction of progradation was generally northward against a
relatively static shoreline. Loci of deposition shifted
constantly in a seaward direction with each wedge of detrital sediments passing through a cycle of subsidence, stagnation, and transgression during which chemical deposition dominated.
Each "dying" phase was followed by a new episode of active
sedimentation.
INTRODUCTION
Scope of Study
One of the goals of sedimentary petrology is decipher
ing the history of sedimentary portions of the earth's crust. One facet of this problem, and the subject of this study, is reconstruction of depositional environments for a particular
assemblage of Middle Pennsylvanian (lower Allegheny) sedimentary rocks in eastern Ohio. The basic approaches to the study of this thin but highly complex rock unit are analysis
of the spatial relationships of rock types in the field and
detailed study of some of the chemical components (ironstones and limestones). Both approaches lead to a recon
struction of depositional environments of early Allegheny time. The chronological evolution of these environments is integrated and coordinated with the development of litho- facies of comparable age in southeastern Ohio and north
western Pennsylvania.
1
2General Geology
Lower Allegheny strata in eastern Ohio crop out along the west flank of the Allegheny Synclinorium (figure 1).
Allegheny rocks in the southern part of the area dip about 100 feet per mile to the east and in the northern part about 50 feet per mile to the south. Lower Allegheny beds vary in thickness from 50 to 125 feet and consist of a great variety of thin, often discontinuous sandstones, siltstones, shales, coals, "underclays," and limestones which are not grossly
dissimilar to those of the underlying Pottsville and over- lying Allegheny strata. Among detrital rocks, sandstones are more abundant in the south whereas shales and siltstones
are more abundant in the northern part of the area. Marine limestones and other zones bearing marine fossils are more
prevalent in the north than in the south and coal beds seem to be about equally distributed throughout the area.
Published information on the early Allegheny consists
of numerous early reconnaissance, regional, county, economic and general geologic reports. Most of these (Stout, 1916, 1918, 1944; Stout and Schoenlaub 1945; White and Lamborn, 1949; Lamborn, 1951, 1954, 1956; Brandt, 1954, 1956; and
Delong and White, 1963) are purely descriptive and do not
3
79'
O H IO
Pittsburgh PENN.
POST-TALLEGHENY
39-W. VA_
ALLEGHENYOUTCROPAREA30
Figure 1. Allegheny Outcrop Area on Flanks of Allegheny Synclinoriura. Area of study indicated by dashed lines.
deal directly with petrogenesis. More recent investigations
on the Allegheny of western Pennsylvania (Perm, 1962, 1964; Williams and Perm, 1964; and Bergenback, 1964) deal with the genesis of the rocks in that area and an unpublished disser
tation by Webb (1963) and unpublished, field data by Flores
deal with aspects of the Allegheny sedimentary development of southern Ohio. Also, the Ohio Geological Survey files contain a considerable volume of descriptive data on lower Allegheny strata of eastern Ohio. All of these sources of information were heavily drawn upon in providing the strati-
graphic synthesis given in the following pages.
LITHOSTRATIGRAPHY OF THE LOWER ALLEGHENY
The spatial distribution of the various rock types of
the lower Allegheny was determined by field investigation and by collection of written records and literature study.
In addition to stratigraphic sections taken from published and unpublished sources, 58 sections were measured in the
field and previously measured sections were re-examined and modified when necessary. Most newly measured sections (see appendix) are located in northern Ohio where stratigraphic control was inadequate. All sections were plotted on stan
dard log strips at a vertical scale of 1 inch equals 10 feet and indexed by 15 minute topographic quadrangles (Plate I).
Correlation and spatial distribution of rock types were
illustrated by stratigraphic cross sections constructed from
the log strips spaced horizontally at the scale of 1 inch
equals 4 miles, then photo-reduced to vertical and horizontal scales of 1 inch equals 20 feet and 1 inch equals 2 miles, respectively (Plates II through VI).
A generalized description of lithic types, stratigraphic names, and geographic location of lower Allegheny strata is
shown on figure 2. The stratigraphic names used in this report are applied only to rock units of at least subregion
al lateral continuity and conform to the current nomenclature of the area. Modification of existing terminology or
creation of new stratigraphic names are not regarded as pertinent to this study. The terms upper and lower Clarion are in accord with Williams' (1959) designation of this unit
as the clarion Formation in western Pennsylvania and with Stout's (1916) reference to this unit as the Clarion shale. The base of the Vanport limestone of northeastern Ohio is
used herein as a convenient stratigraphic position for dividing the Clarion Formation into lower and"upper parts (figure 3). Because of some ambiguity in correlation in
southern Ohio and northeastern Kentucky, Webb's (1963) terms, "lower Allegheny" and "Allegheny" are retained.
General Description of Lithic Types
Krynine (1954) subdivided sedimentary rocks into two
litho-genetic groups— detrital and chemical. The Clarion
Formation of eastern Ohio contains several members of both
basic groups. Detrital rocks are composed primarily of
clastic silicates which were carried into the basin of
O H I OFIGURE 2
SCHEMATIC CROSS SECTION O f B s o c k s i n mm o h k
SOCKS O f A llEG HENY AGE
O W ER K IT TA N N IN G COALALLEGHENY SAN D5T0N ES SILISFONES, AND SHALES
ooiriflo rrom r r e o o . 1
UPPER CCL A RIO NSA N D S ICOAL
A N D
VANPORT LIMESTONELOWER CLAR O NCOALLOWER ALLEGHENYFLINT SA N D S TO N ES, SILTSTONES
SA N D STO N ES, SILTSTONES A N D SHALESA N D SHALES ZALESKO G A
M FLINCOAL
6ROOKVILLE COAL
ROCKS O r POTTSVILLE AGE
MILES
O H I O PA.FIGURE 2
SC HEM ATIC C R O S S S E C T IO N O f LOWER ALLEGHENY R O C K S IN EASTERN O H IO
R O C K S O F ALLEGHENY AGE
LOWER KITTANNING COAL
LOWER K I llA N N lN G IINDERCLAY* 1
miE C O A L TTr~H
FEET r75
S A N D S T O N E S , S IL T S T O N E S , A N D SH A L E S
L O W E R C L A R IO N S A N D S T O N E S , S IL T S T O N E S
A N D SH A L E S
W IN T E R SC O A L
Z A L ESK I T
P U T N A M HILL L IM E S T O N E B R O O K V IL LE C O A L
• 5 0
■25
LO
R O C K S O F POTTSVILLE AGE
o 2 0 4 0i— — jM ILES
8
I- i• i
!
Figure 3. Outcrop of the Clarion Formation in northeastern Ohio (TJhrichsville no. 14 section) . a - Brookville coal; b - Putnam Hill limestone; c - lower Clarion; d - upper Clarion; e - Vanport limestone.
deposition as solid particles derived from a distant source. Size classes represented range from coarse sand to clay. Chemical rocks are composed of materials generated chemi
cally by inorganic or biogenetic processes within the area of deposition. Clarion chemical rocks which are composed of primary organic and chemical components are coal, some chert, ironstone, and limestone whereas those of secondary origin (altered from other rocks) are residual chert and some
"seat rock" (commonly referred to as underclay).
Detrital Rocks
The major detrital rocks are sandstone, siltstone, and
claystone, each size class presumably reflecting decreasingo
hydraulic energy.
Sandstones
Most sandstones are composed of very fine to fine
grained sand and occur in solid units less than ten feet in thickness. Sandstone units with thicknesses on the order of tens of feet commonly have coarser grain sizes at the base and become finer upward.
Most of the sandstones are low rank graywackes containing about 50 percent quartz, 30 to 40 percent micaceous rock
10fragments, and minor amounts of clay minerals and other con
stituents (Webb, 1963). Orthoquartzitic lenses occur within some of the thicker sandstone beds.
Freshly exposed sandstones are commonly light to medium
gray presumably reflecting the unaltered color of the mineral components whereas weathered exposures are generally light tan or buff, probably due to oxidation of iron bearing minerals.
Siltstone and Silty Shale:Siltstone and silty shale make up the largest propor
tion of lower Allegheny detrital rocks. Nearly all silt
stones contain a considerable quantity (20-50 percent) of
clay size material and where the clay size fraction exceeds
that of silt, siltstone grades into silty shale. Within the lower Allegheny most siltstones occur beneath or are laterally equivalent to sandstone and contact relationships
are commonly gradational.
In terms of mineral composition most of the siltstones are low rank graywackes. The silt size fraction is mostly
quartz whereas the clay fraction is predominantly hydromica (mostly illite). In many outcrops ironstone (siderite)
nodules and layers, generally less than 4 inches thick, are
11dispersed throughout the silty shales and, to a lesser
extent, in the siltstones.Fresh exposures of siltstone and silty shale are usually
various shades of gray. Particle size and bedding charac
teristics are important factors controlling color. Dark grays seem to indicate an abundance of very fine grained clay mineral particles whereas lighter grays commonly reflect
coarser sizes. Weathered siltstones are generally light gray or buff due to oxidation of iron bearing mineral com
ponents.
Claystone:Claystone refers to very fine grained rocks composed
mainly of clay-size constituents. In this report the term
clay shale is used synonomously with claystone since it is
a more descriptive term referring not only to grain size but
also to degree of cleavage and/or bedding. The majority of
lower Allegheny clay shales contain between 20 and 50 per
cent silt-size material and commonly grade upward or laterally into silty shale.
Hydro-micas and kaolinite make up most of the clay-size
minerals but small amounts of quartz and other detrital
minerals are also present. Ironstones, which are common in
. 12silty shales, are also abundant in clay shales. Marine and
brackish fossil debris contributes calcareous material to
the shales, especially in zones directly overlying coal beds or limestones.
Clay shales.are usually darker than silty shales and, where finely divided plant debris is abundant, the rock is
often very dark gray or nearly black. The unweathered out
crops of some sparsely fossiliferous clay shales are green
and usually become gray with continued *exposure.
Chemical Rocks
The chemical rocks of the lower Allegheny can be sub
divided on the basis of mineral composition and among limestones grain and/or crystal size is a suitable criterion for
further subdivision.
Coal;
Lower Allegheny coals are composed of bright vitranous bands (presumably resulting from large woody plant tissues) and dull layers of finely macerated plant material, pyritized plant debris, or shaly partings. The coal is of bituminous
rank and occurs in-beds ranging in thickness from less than
1 inch to 6 feet. Stratigraphic positions of these coals
are indicated on figure 2 .
Seat Rock;
Lower Allegheny seat rock (underclay) is composed of clay minerals as well as some carbonaceous matter and quartz.
The principal clay minerals are probably similar to those of Pennsylvanian underclays in Illinois which are composed of illite, mixed-layer illite-montmorillonite, and illite-
montmorillonite-chlorite (Schultz, 1958). Most of the
clayey seat rock is plastic, with colors of light gray or
cream mottled with dark shades of gray, brown, or purple.
Much of the carbonaceous material is in the form of root
fossils, indicating that seat rock is probably ancient soil.
Root penetration has destroyed stratification and dark organic pigments common to other fine grained rocks seem to have been destroyed by leaching.
ChertsLower Allegheny cherts appear to have diverse origins;
some .probably formed from solidified amorphous silica gel, whereas others appear to be definitely the result of concentrations of organic spicules. A small quantity are secon
dary, replacing some limestones and filling vugs in others.
14Chert occurs in three stratigraphic positions. The
lower two— Kilgore and Zaleski (figure 2)— are composed pri
marily of siliceous sponge spicules matted together in a silica-cemented quartz silt matrix (Webb# 1963). The third stratigraphic occurrence of chert is the Vanport limestone of northeastern Ohio (see figure 2). Most of this chert in the ''northern" Vanport seems to be composed of chalcedony and small amounts of micro-crystalline quartz. Stout and
Schoenlaub (1945) report that one sample from this unit was composed of 99 percent silica.
Ironstone;
Ironstones are common minor components of lower Alle
gheny clay shales, silty shales, and siltstones. They are
composed primarily of siderite and clay minerals and most
occur in bands or layers less than 6 inches thick. A few
occur as discoidal, ellipsoidal, and globular forms (verti
cal thickness usually ranges from 0.5 to 6 inches) randomly distributed throughout the host rock. Most nodular forms
are enclosed in strata that drape over and under the concretions without disturbance of the individual laminae.Other forms commonly have laminae that continue through the
nodule without any major change. In the latter type laminae
15adjacent to the nodule are in some instances more compacted
than those within the nodule. Such an arrangement of mor
phological features with respect to host rock suggests that ironstones became relatively non-compactable before the
surrounding rock.
Limestone;Fossiliferous marine limestone occurs at two strati
graphic positions in the lower Allegheny. The lower of the two is the Putnam Hill, the basal marine unit of the Allegheny throughout most of Ohio (figure 3). The Vanport
limestone of northern Ohio occurs about 15-50 feet above the Putnam Hill or approximately midway between the Brookville and lower Kittanning coal beds. The Vanport of southern Ohio occurs about 20-40 feet above the Brookville coal bed
and directly above the "Clarion11 coal bed (figure 2) .The Putnam Hill limestone is very dark gray, clayey,
and usually has a constant thickness of about 2 feet. The
Vanport limestone of both southern and northern Ohio is
light to dark gray, commonly siliceous, and more variable
in thickness (20 feet or less) and is laterally less persist
ent than the Putnam Hill.
16Spatial Distribution of Lithic Types
The various rock types of the lower Allegheny in Ohio have a systematic albeit complex spatial arrangement. In
southern Ohio (south of 39° 30' N. latitude) Webb (1963) has
described two offset wedge-shaped sedimentary units overlain
by a third which overlaps both subjacent wedges (see figure
2). Webb has ascribed the offset and overlap relationships
to deltaic progradation and shifting. The northernmost of
Webb's two lower deltaic wedges expands greatly in northern
Ohio and Pennsylvania where they represent the Clarion
rocks of this study. Variation in thickness of this unit and its components is shown on cross sections (Plate II through VI) and figure 2. Clarion rocks are thin (about 20 feet) along the northwest outcrop and have the greatest thickness (about 100 feet) along the east and southeast edge
of the outcrop. Most of this variation is due to thickening and thinning of the detrital members.
Stratigraphic Components of the Clarion Formation
North of 39° 30' N. latitude the Brookville coal, the
basal Allegheny unit of northeastern Ohio, is apparently
ubiquitous, seldom exceeding 4 feet in thickness and
17generally averaging 1.5 to 2 feet. The Brookville is either
directly overlain by the Putnam Hill limestone or separated from it by a few inches of fossiliferous shale. The Putnam Hill is a sheet-like, clayey, fossiliferous, limestone averaging approximately 1.5 to 2 feet in thickness. Thicker
limestone occurs at a few localities around the outer peri
phery of the outcrop, especially around the northwest edge
of the arcuate outcrop in northern Ohio.The detrital rocks which overlie the Putnam Hill
generally contain marine-brackish fossils (chonetids and pro
duct id brachiopods are.abundant) at the base and show a verti
cal decrease in fossil abundance accompanied by a correspond
ing increase in finely disseminated plant debris. These
rocks generally contain abundant ironstones and commonly grade upward from clay shale at the base to silty shale or
siltstone at the top.The Vanport limestone overlies the lower Clarion detri
tal rocks. Though much less laterally persistent and litho-
logically consistent than the Putnam Hill, it is in most places a fossiliferous marine limestone or chert. It is
relatively thick (5 to 15 feet) and predominantly pure lime
stone around the northwest and northern part of the area.
18Toward the southeast edge of the outcrop belt (structurally
down dip) it occurs as erratic pod-like bodies from a few inches to 18 feet thick and contains quartz and chert impurities. In some sections, e.g., Uhrichsville no. 14 and Conesville no. 18 (see Plate II) siliceous mineral components comprise a minor, but important, portion of the rock; still further south in the Frazeysburg quadrangle the Vanport is
predominantly chert.Upper Clarion detrital1 rocks are quite similar in
lithology to the detrital rocks of the lower Clarion. Most of these rocks contain abundant ironstones but rarely have
marine fossils. Vertical and/or lateral gradation of clay• r
shale or silty shale to siltstone is common. The upper
Clarion stratigraphic interval apparently thickens to the
east with an accompanying increase of detrital components.The Lower Kittanning underclay forms the upper boundary
for the upper Clarion detrital rocks. Although variable in thickness,"the underclay is usually present and in some
cases occupies most of the interval between the Vanport and the lower Kittanning coal (see Frazeysburg sections on Plate
II) .
19Summary and Working Hypotheses
The spatial arrangement of lower Allegheny rocks in
eastern Ohio illustrates relatively thick units of detrital rocks bounded by relatively thin units of chemical rocks (Plates IX through VI). Within the detrital units there is
a general gradation from fine-grain size at the bottom to coarse at the top. These characteristics are similar to
those of Allegheny rocks in northwestern Pennsylvania which Williams and Ferm (1964) ascribed to detrital wedge-shaped units typical of deltaic deposition. Similar lithic
sequences in the modern Mississippi River Delta (Coleman and Gagliano, 1964) further substantiate deltaic origin of
lower Allegheny sediments."Active" and "passive" processes of early Allegheny
deposition are reflected by detrital and chemical rocks, respectively. Presumably, detrital rocks reflect the effect
of active delta progradation whereas limestones, coals and seat rocks reflect less dynamic sedimentation during delta
stagnation and decay. Two combinations of these gross environments of deposition are sufficient to explain the mode of accumulation for the bulk of lower Allegheny rocks. These are (1) a prograding detrital wedge coupled with a
20regressive shoreline— the chemical rocks (limestones) of this
environment were deposited basinward away from the influence
of the prograding wedge (figure 4); and (2) a static detrital
wedge coupled with a transgressive shoreline— limestone, chert, seat rock, and coal of this environment were deposited
on the flanks and/or upper surfaces of the static wedge (figure 4). The lateral shifting of prograding wedges, a trait common to delta deposition the world over, appears to have been followed by stagnation, decay, and transgression
of each preceding wedge.Although the "depositional models11 of figure 4 depict
the probable environments in which lower Allegheny rocks
were deposited, additional data of a more specific type is needed to supplement and support these general contentions.
Two lines of evidence have already been applied on the
equivalent rock unit in northwestern Pennsylvania, chemical content and petrography of carbonate components (Weber and
Williams, 1965) (Bergenback, 1964). The following sections
of this report deal with similar evidence from the lower
Allegheny rocks of eastern Ohio.
21
DEPOSITIONAL MODELS
EX PLA N A TIO N
M SANDSTONE H SILTSTO N E m SHALE EHPUNDERCLAY' E 3 CHERT r a LIMESTONE ■ COAL
PROGRADING DETRITAL WEDGEREGRESSIVE SH O RELIN E■ >
DETRITAL W E D G E S
STATIC DETRITAL WEDGE TRANSGRESSIVE SH O R E L IN E
DETRITAL W E D G
Figure 4. Depositional models applicable to the genesis of lower Allegheny rocks.
DETAILED STUDY OP SOME LOWER ALLEGHENY CHEMICAL ROCKS
Introduction
Among the most conspicuous chemical rocks of the lower
Allegheny are ironstones, disseminated in shales and silt- stones, and the two limestone units, Putnam Hill and Vanport. Analysis of these two rock types comprise an independent test of hypotheses based mainly on general lithology. Ironstones were treated mostly by spectrochemical technique whereas limestones were studied petrographically.
Ironstones
Using spectrochemical techniques, Weber and Williams
(1965) have shown that the Si02 content of Allegheny iron
stones is greater in freshwater than in marine nodules
whereas vanadium is relatively more abundant in marine than
in freshwater nodules. In order to determine whether these
criteria are in accord with general lithostratigraphic data,
samples were collected and analyzed from 16 stratigraphic
sections representing the spectrum of geographic and litho- logic variation. Specific locations of samples are shown on
23figures 5 and 7 and a typical sampling locality is shown on figure 6.
A record was made of the physical characteristics ("size," shape, lime contents, included fossils,’*' and the
type of enclosing rock) for each sample. Preparation of ironstone samples for chemical analysis consisted of remov
ing the external "weathered" portion of each nodule, col
lecting about 3 grams of fresh core material, and pulveri
zing it in a commercial high frequency vibrator-grinder to a
particle size less than 300 mesh. Elemental silicon content
was determined by neutron activation analysis at the
Louisiana State University Nuclear Science Center, but
mechanical limitations of the analyzing equipment did not permit a vanadium analysis. Results of the silicon analysis are shown on table I .
Limits for salinity categories based on silicon content
are modified from Weber and Williams as follows: (1) freshwater— greater than 14.8 percent silicon; (2) marine— less than 2.6 percent silicon and (3) brackish— 2.6 - 14.8 percent
T}
■*-In addition to fossils within ironstones, H. H. Roberts made a complete census of the fossils found in seven of the stratigraphic sections and presented the results in a M.S. thesis at Louisiana State University (Roberts, 1966).
24
• 70 Stratigraphic Section & Number (see appendix for description) • 2
o 1219
H O
HOM
W
OHIO
Figure 5 Index map of 15 minute quadrangles showing chemical rocksampling localities.
25
FEB •
Figure 6. Ironstones in the upper Clarion at the Newcastle no. 2 section. a -ironstone concretions; b - silty shale.
26Table I. Silicon content in ironstone concretions.
Beaver 2 4 6.72*Location of section shown in figure 5. See the appendix for stratigraphic description.
**Samples numbered from bottom to top of stratigraphic section.
28
silicon. Figure 7 shows the interpretation of environments,
based on silicon analysis, along a line of lower Allegheny section extending across eastern Ohio and western Pennsylvania.
Silicon Content and Paleogeographic Inferences
At least two depositional factors probably contribute
to the variation in silicon content of ironstones: (1) the proportion of freshwater entering the depositional site; and
(2) the average grain size of the sediment being deposited. The silicon content of freshwater exceeds that of marine
water, therefore, ironstones from a freshwater environment probably would contain more chemically precipitated silicon than those deposited in a marine environment. In addition most ironstones contain some detrital material and where
this detritus is coarse grained, quartz is a dominant com
ponent. Thus ironstones which occur in coarser grained detrital rocks may be expected to have a somewhat higher
silicon content than those associated with finer grained sediments.
The largest portion of samples fall within the brackish
category (see table I and figure 7). Such results are in
* * * *
%\i % % .%
HU wM
a w »SI
< mterttltttt" %
m
W >
5£i**2
l < \ W
OkmwA
« u
»
VpP
HW
30accord with- anticipated brackish environments with fluctua
ting salinity conditions accompanying prograding deltaic sequences. The depositional environments for the detrital rocks were probably comparable to those depicted by the
"prograding detrital wedge model" of figure 4. This result of predominantly brackish environments is supported by a
study of fauna variation of the lower Allegheny (Roberts, •
1966). However, certain ironstone silicon data indicate a
marine depositional environment for lower Clarion detrital
rocks along the northern outcrop area (see Canton no. 8 and Alliance no. 15 sections on figure 7).
Limestones
The Putnam Hill and Vanport limestones of the north
eastern part of the study area were examined petrographically
in order to characterize and compare the two limestones in terms of probable mode of deposition.
Limestone samples were collected at 14 stratigraphic
sections (table II and figure 5) which, like the ironstone sections, represent a wide variety of rock type and broad '
geographic distribution. The Putnam Hill and Vanport both
were sampled at 4 outcrop sections whereas 6 sections were
31Table II. Index to limestone samples.
15 minute cuadr ancile
Stratigraphic section and sample number*
Limestonesampled
LSU thin section no.
New Lexington 17-1 Putnam Hill 2387Zanesville 31-1 Putnam Hill 2388Conesville 18-1 Putnam Hill 2389Conesvilie 18-9 Vanport 2391Uhrichsville 14-1 Putnam Hill 2393Uhrichsville 14-16 Vanport 2397Dover 19-1 Putnam Hill 2398Navarre 24-1 Putnam Hill 2399Newcomer stown 14-1 Putnam Hill 2400Newcomer stown 2A-1 Putnam Hill 2401Canton 8-1 Putnam Hill 2402Canton 8-3 Putnam Hill 2403Canton 8-7 Vanport 2404Canton 8-8 Vanport 2405Canton 8-9 Vanport 2406Alliance 15-1 Putnam Hill 2407Alliance 15-5 Vanport 2408Beaver 2-2 Vanport 2410Beaver 2-3 Vanport 2411Beaver 12-1 Vanport 2412Beaver 7-3 Vanport 2413Newcastle 2-1 Vanport 2414Newcastle 2-2 Vanport 2415Newcastle 2-3 Vanport 2416Newcastle 2-4 Vanport • 2417
*Location of section shown in figure 5. See the appendix for stratigraphic description.
sampled only for the Putnam Hill and 4 were sampled only for the Vanport (table II). In order to evaluate small scale horizontal and vertical variation, samples were col
lected in pairs, separated horizontally by at least 3 feet
and vertically by not more than 3 feet. This sampling
32procedure yielded 60 samples— 24 from the Putnam Hill, the
remainder from the Vanport.
Acetate peels were made of all samples and examined
under a binocular biological microscope. Prom this examination, 25 representative samples were selected for thin-
sectioning (11 from the Putnam Hill and 14 from the Vanport).
Petrographic Analysis
The classification of limestones used in this study is
basically the same as that proposed by Polk (1959) with the
exception that limits of size categories are slightly modi
fied. Four lithic limestone components and three other
components (generally detrital or authigenic non-limestone material) were differentiated. The limestone components
are micrite, microspar, spar, and bioclasts. The first three members of this series are differentiated on the basis
of particle size and the fourth, bioclasts, are as the term
indicates, clastic particles of known organic origin. Some
attributes of the petrographic components are shown on table ill.
33Table III. Limestone nomenclature
Calcium Carbonate ComponentsBasic Elements Subdivisions
Micrite (microcrystalline carbonate 4 microns or less in diameter) micrite aggregates intraclasts
pellets■Su4Js
reorganized or recrystallized micrite
Microspar (spar between 4 and 10 microns in diameter)
microsparaggregatesfilling hollow fossils, fissures, and interstitial areas
intraclastspellets
may be in mosaic form
u
reorganized or recrystallized microspar
Spar(spar 10 microns or more in diameter)
filling hollow fossils, fissures, and interstitial areasovergrowths on fossils and components of reorganization (recrystallization of bioclastic material and microspar
A A A < A A A A Limestone Unit*IO to top- p» p» toP-
to to to to p- p- p- p» Sample Numberm m Ui P* CO to H O
7677 59 00CO
75737267 MatrixI-1 1—1 to to Pellet KH*O
Intraclast Hrift)
7677 66 00
4>OV “O 'O ■o OO P W M • Total
P* to 111 MatrixCO C\ Ot 00 I-* Cement sH*O . H
Pellet O CO . ^
00 Ov VO I-*o I-* to -o Total (0H
MH O' H to 1-*p* I—1 1—1 t—1
Spar
m c \ to CO to to to Echinodermto to t-» BrachiopodCO CO t—* Pelecypod
t-* Gastropodto I-* Foraminifer td
t->-l-> Ostracod oo
Bryozoan pcorrCoral co
COtoo Algae
1-* t-1 t-»
106 Unknownt-*on vo co p-
I—* toO "O H P Total
t-» t-» Quartzt—1 Chert
t-»co to Cn Clayi—1 h-* t—* I—* Pyrite Oft
P> t-1 Siderite Ct*(Dn
t—1 Limonite CO
Unknown’ t-* to t-J 'Woody Material1
t-»P t O H o 1388 Total^ 9E
Table IV.
Continued
37
Figure 8. Photomicrograph of section 2397. a - "micrite" intraclast; b - ostracod; c - quartz in micrite matrix.
Figure 9. Photomicrograph of section 2414. a — "micrite" pellets; b — microspar cement surrounded by micrite matrix.
38
Figure 10. Photomicrograph of section 2403. a - spar cement; b - bryozoan fragment; c - "encrusting" foraminifer.
Figure 11. Photomicrograph of section 2415. Nicols crossed, a — siderite replacing sparry calcite; b — microspar; c - micrite.
39
Figure 12. Photomicrograph of section 2411. a - algal fragment (note the microstructure) y b - tan spar mosaic; c - tan microspar mosaic.
Figure 13. Photomicrograph of section 2416. a - echinoderm fragment replaced by quartz; b - authigenic quartz; c — "brachiopod"? spines.
40
Figure 14. Photomicrograph of section 2393. a - echinoderm fragment; b - pelecypod fragment; c - brachiopod? fragment; d - "microspar" pellets susrounded by pyrite.
Figure 15. Photomicrograpli of section 2399. a — bryozoan fragment; b - "encrustirig" foraminifer; c - gastropod fragment; d - coral? fragment.
413 Putnam Hill and 10 Vanport samples and micrite intraclasts
occurred exclusively in two Vanport samples (sample nos.
2397 and 2408). In the latter two samples, pellets and bio
clasts are very scarce.
Microspar sMuch of the Putnam Hill and Vanport microspar appears
to be cement but some is probably slightly recrystallized
matrix (e.g., sample no. 2406). Pellets of microspar are
minor constituents in both limestones. Some pellets with cores of microspar surrounded by pyrite (figure 13) may be
fecal with the core material representing reorganized or recrystallized micrite and the encasing pyrite represent
ing remains of undigestable organic material.
Spar:Sparry calcite seems to be about equally distributed in
both of the limestones. It occurs as void filling in
fossils, fissures, and interstitial areas, as overgrowths on
fossils, and as recrystallization products of microspar and
bioclastic material. Some spar mosaics, comparable to those reported by Bergenback (1964) in the Vanport of western Pennsylvania, were identified as algal fragments. Most
42bioclasts, however, when recognized as such, were differen
tiated on the basis of taxonomic grouping rather than particle size.
Bioclasts:
Fossil fragments are distributed throughout the Putnam
Hill and Vanport limestones; however, proportions of indi- -
vidual taxa are not large enough to bring the estimates
under statistical control. Identifications were made on several levels; echinoderms (mostly crinoid columnal segments) , brachiopods, bryozoans, coelenterates (corals),
and algae are classified at the Phylum level. Pelecypods, gastropods, and ostracods are classified at the Class level.
Foraminifers, including fusilinids and encrusting forms, are grouped at the Order level.
Alcrae appears to be the most abundant bioclastic material
(table IV) in the two limestones, and very probably the "unknown" category contains many unidentifiable algal fragments. Some of the algal material is in the form of spar
mosaics in elongate, curvilinear stringers, some appears to
be in a growth position in the manner of encrusting forms, and still others ('blades') appear to have been fragmented
and deposited in ooze and bioclastic debris. Nearly all
43isamples of the Putnam Hill of Ohio have some algal fragments
whereas such material is not found in the Vanport. Two samples (2411 and 2417) of the Vanport in western Pennsyl
vania, however, do contain algal material.Echinoderm fragments are generally the second most abun
dant fossil element (table IV), but in most of the Putnam Hill samples foraminifers (mostly encrusting forms) are more
abundant than echinoderms. Fusilinids are relatively abun
dant in many of the Vanport samples, but are less conceft-
trated in the Putnam Hill. Greatest abundance of Vanport
fusilinids is usually associated with intraclastic material and such material often occurs near the top of the limestone unit. Next to echinoderms pelecypod fragments are the most
abundant bioclasts. ' Most pelecypod shells were disarticulated when the organisms expired, and subsequent fragmenta
tion was more severe than for the brachiopods. Thus in hand specimens brachiopods seem more abundant than pelecy-
pods.Brvozoan fragments (figures 9 and 14) are apparently
more abundant in the Putnam Hill than in the Vanport (table IV). Complete or unbroken bryozoan fronds rarely occur in
either of the limestones, and most fragments are brown-
colored or replaced by pyrite.
44Brachiopods. gastropods. ostracods, and corals are all
sparsely and about equally distributed in the Putnam Hill and
Vanport. Corals, especiallyoccur in such small amounts that they are relatively insignificant contributors to the
total bulk of the carbonates. Unknowns (unidentified material) comprise a large quantity of the bioclasts (table
IV). Subjectively, most of this material was ranked as algae, brachiopods, and pelecypods.
Other Components;Quartz, chert, and clay are the silica minerals in the
Putnam Hill and Vanport. No quartz nor chert was recorded for any of the Putnam Hill samples although a considerable
amount of silt-size quartz (16-17 percent) is present in some
Vanport samples (nos. 2391 and 2397). Very little quartz or chert occurs in Vanport samples from western Pennsylvania, however some authigenic quartz replaces carbonate (micrite and bioclasts) in one sample (see figure 13). Minor amounts of chert, some detrital and some in mosaics filling pores,
were found in a few of the Vanport samples.Clay minerals are present in a few samples. Though
lime mud and clay, when mixed, are difficult to differentiate, field observations, and to lesser extent petrographic
45data, indicate a considerable quantity is present in most
of the Putnam Hill limestone.Authigenic pyrite. siderite, and limonite comprise the
"iron minerals'* which occur in small quantities in the two limestones (table IV). Pyrite, the most abundant, is dis
seminated as separate small (less than 10 microns) crystals and clusters of crystals throughout micrite and it appears
to reach maximum proportions when woody plant debris is
also present. Occasionally bioclasts are replaced by pyrite, and in some instances the spar filling of intrastital
voids is replaced.Siderite is present in several of the thin sections.
Though quite rare, it appears as the replacement product
of individual crystals of calcite (figure 10). Tan-colored
microspar and spar comprising algae in several samples also may be siderite. Limonite appears in small insignificant
quantities as a replacement or alteration product of both
pyrite and siderite.Organic woody plant material is widely disseminated
throughout much of the two limestones. However, the fine grained nature of the material and its association with pyrite in "muddy'* limestone makes unequivocal identification
46difficult.
Petrographic Summary and Paleogeographic Inferences
In a petrographic sense, the Putnam Hill and Vanport
limestones are biomicrites according to Folk's (1959) class
ifications and both limestones apparently contain comparable
amounts of micrite. The source of the micrite is uncertain, but if the estimates of algae and echinoderms are correct these may have provided a sizeable biologic source. Mechan
ical abrasion of other organic debris along with chemical
precipitation probably added to the supply. The major petrographic difference between the two limestones is the presence of intraclasts, detrital quartz, and chert in the Vanport and its absence in the Putnam Hill. Furthermore within the Vanport the amount of detrital silica diminishes
from about 15-20 percent in the southern part of the out
crop to 5 percent or less in northern Ohio and western Pennsylvania.
Although both the Putnam Hill and the Vanport are
obviously of marine origin, certain differences in gross
lithic relationships are apparent. Over most of the out
crop in northeastern Ohio the Putnam Hill directly overlies a nonmarine deposit (Brookville coal) whereas the Vanport
47overlies brackish or brackish-marine rocks. The Putnam Hill
is in turn overlain by marine to brackish marine rocks whereas the Vanport is overlain by brackish or brackish- nonmarine (freshwater?) rocks. These stratigraphic relationships indicate two different transgressive situations; the
Putnam Hill analogous to the lower limestone of the "static detrital wedge model" (figure 4), and the Vanport analogous
to the upper limestone of the same figure.
The Putnam Hill limestone probably was deposited in a
shallow marine sea which was relatively free from the influx
of coarse detritus. Static conditions of deposition are suggested by the conspicuous absence of quartz and the abundance of clay, especially in outcrop sections where clay
partings in the limestone are frequent (see stratigraphic descriptions in the appendix); and the widespread uniformity of lithic character and constant thickness over a large
area.The Vanport limestone was probably deposited in a shal
low marine embayment which had a more irregular outline, pronounced bottom topography, and higher energy conditions
than those of the Putnam Hill. Very rapid thickening and
thinning (e.g., see Uhrichsville no. 14 and Dover no. 1 in
Plate 2), unrelated to erosion, is suggestive of irregular
bottom topography and/or irregularity of the basin margin.
Higher energy conditions for the Vanport are suggested by the general lack of orientation of bioclasts in contrast to the very well developed bedding in the Putnam Hill limestone.
Finally, that these conditions of greater energy were associated with minor detrital influx from the south is indicated by the increase of coarse-grained silica detritus from north to south. Over all, most of the Vanport in eastern Ohio was deposited as isolated patches of bioclastic material
partially mixed with detritus from waning distributaries on the static portion of a detrital wedge. Vanport deposits
along the northern rim of the outcrop in Ohio and western
Pennsylvania reflect deposition further off shore in a
relatively shallow shelf zone with bottom irregularities.The minor anomalies of the seafloor topography, though probably reflecting earlier Allegheny and/or Pottsville deposi- tional patterns, may have been bottom features upon which
marine invertebrates and algae could grow and contribute
to the bulk of carbonate deposition.
RECONSTRUCTION OF DEPOSITIONAL ENVIRONMENTS
Introduction
Previous chapters have dealt with the kind and amount of lower Allegheny data and certain interpretations and inferences drawn from the different types of data. .In
this chapter this information is synthesized and an interpretation is made of the lower Allegheny sedimentary history of eastern Ohio. In this interpretation the previous works of Williams and Ferm (1964) in western Pennsylvania; Ferm
(1964), Zimmerman and Ferm (1965) in Ohio; and Webb (1963)
in southern Ohio are drawn upon in order to achieve a
regional synthesis.The evolution of the lower Allegheny sedimentary pat
terns is illustrated by a series of paleogeographic maps
(figures 17 through 21) depicting geographic location of
major progradational phases and associated environments.The vertical dimension of the sediments deposited in these
environments is illustrated schematically by an accompanying stratigraphic cross section (figure 16).
Figure 16. Schematic cross section showing major phases of progradation in eastern Ohio.
SCHEMATIC CROSS SECTIONOHIO
LOWER KITTANNING COAL
VANP6RfMMEWNE
w m .WM A PHASE 2 PHA$EPHASE 1%9pAP H A S E RN W W W S N N N 'XXU.TNAM2HJLL LIMESTONE
BROOKVILLE COAL BROOKVILLE COAL
H COAL & 'UNDERCLAY' BRACKISH-NON-MARINE£ Y
MILES
ISHALE, SILTSTONE & SANDSTONE
LOWER ALLEGHENY EASTERN OHIO
MARINE BRACKISH SHALE
H MARINE SHALE & LIMESTONE
□ CHERT
V
Figure 17. Early Allegheny paleogeography? phases 1 and 2.
S tag n an t N o n -M a r in e Deposition
N o n - M a r in eDeposit ion
Static W edge
Slowly P ro g rad in g W e d g eRapidly Prograd ing W ed g e
S tag n an t M a r i n e - Brackish Deposit ion
M ar ine-Brack ish Silt and Clay
M ar in e Limestone
H E R
▼ A
EARLY ALLEGHENY PALEOGEOGRAPHY
PHASES 1 & 2
30I
MILES
44889
Sedimentary Development of the Lower Allegheny
54
Initial Allegheny deposition in southern Ohio was in
the ’'Brookville” peat swamp. Figures 16 and 17 illustrate
this swamp and its western Pennsylvania equivalent, the lower Clarion, which developed on older (Pottsville?) subsiding deltaic wedges, one of which is shown on figure 17 as the Kilgore wedge of phase 1. This swamp was transgressed in southern Ohio by Clarion marine sediments which form the basal rocks of the prograding brackish-nonmarine wedge. This detrital wedge (phase 2) gradually prograded
and shifted northward partially overlapping transgressive
deposits (Putnam Hill limestone) that were laid down over the Brookville and lower Clarion peat swamps. Near the Ohio-
Pennsylvania line a small detrital wedge prograded southward.
The prograding system of phase 2A on figure 18, now
represented by lower Clarion rocks in south central Ohio,
apparently had loci of deposition farther north than the previous wedges. The maximum outcrop thickness of this
wedge exceeds 60 feet. Two lobes of the detrital wedge developed the northern one probably resulted from a shift of the prograding system. The area to the south was
static and topographically high. During the early part of
Figure 18. Early Allegheny paleogeography? phase 2A.
m
N on-M ar ineDeposit ion
Sta tic W e d g e
Slowly Prograding WedgeRapidly Prog rad ing W e d g eMarine-Braclcish Silt and Clay
M ar ine Limestone
EARLY ALLEGHENY PALEOGEOGRAPHY
PHASE 2A
57
phase 2A, the Putnam Hill carbonate sediments continued to accumulate, fringing the northwest shoreline. Farther to
the east, in Pennsylvania, the detrital wedge from the
north was the site of increased southward progradation.During phase 3 (figure 19) active progradation shifted
farther northward depositing a marine-brackish wedge of lower Clarion sediment in northeastern Ohio that has a maximum outcrop thickness of over 40 feet. Sedimentary patterns of this phase are very complex. The prograding wedge fed from a distant southern source and covered a large area. This is reflected in the apron-like distribution of the marine-brackish shale. Only minor sandstone channel deposits are found in the sequence.
Contemporaneous with the gradual shift to the north
east and northward growth, the older southern wedges gradually stagnated and the oldest wedges became sites of peat
swamps. These swamps, now represented by the clarion coal
of southern Ohio developed as far north as the south side of
the wedge of phase 2 (see figure 16). Subsequently the
area subsided and the "southern" Vanport, a transgressive limestone, was deposited. This marine limestone grades
laterally toward the north, east, and south into brackish shale and chert which probably indicates the landward edge
Figure 19. Early Allegheny paleogeography; phase 3.
60of the transgression. In western Pennsylvania, the detrital
wedge of phase 2A became static and it too was covered around
the fringes by peat swamp.During phase 4 (figure 20) coarse detritus was shunted
into the detritus-free area over which the "southern" Van
port sea had previously transgressed. This region with its
reduced base-level and close proximity to the avenue of
transport, probably made an ideal site for the accumulation
of detritus in an area extending from the southern part of Ohio northward to the center of the detrital wedge deposited during phase 2 (see figure 16).
The northern areas, sites of deltaic advance during
phases 2A and 3, probably began subsiding and were trans
gressed by the "northern" Vanport sea. Transgressive Vanport limestone was deposited around the northern edge of
the basin and into western Pennsylvania where it attains a
thickness of 20 feet.Phase 5, the last major progradational episode of the
early Allegheny is illustrated on figure 21. During this phase, now represented by upper Clarion rocks, progradation continued northward across the area previously covered during
phase 3. In some places more than 70 feet of upper Clarion
shale was deposited during this phase. Some of this material
Figure 20. Early Allegheny paleogeography; phase 4.
Static W edge
Slowly Prograding Wedge
Rapidly Prograding W e d g e
Chert Where PresentSiliceous Limestone Where Present Limestone Where Present
and data from ironstones included in some clay shales, silty shales, and siltstones, suggest marine or brackish condi
tions whereas other detrital rocks (e.g., most sandstones) seem to be mainly nonmarine. In general, the evidence from these detrital rocks suggests that within thin vertical
rock sequences there are upward gradations from marine to
nonmarine and from fine to coarse size materials, perhaps
indicative of prodelta, shallow bay, and other paralic
sedimentary environments.Rock types resulting from the various depositional
environments may be grouped into sedimentary units composed
of various lithic types. Each lithic type represents a
66
67
certain group of depositional phases. Two sedimentary units
are distinguishable in northeastern Ohio, the lower, and upper Clarion. Additional or comparable units to the south
have been reported by Webb (1963). The lower and upper Clarion units may be referred to the Clarion sedimentary complex where the two cannot be differentiated. Neither
the lithic types, nor the sedimentary units are continuous
over very large distances, and local or sub-regional causes must be responsible for most of the lithologic variation.
Spatial arrangement of the various rock types of
differing lateral continuity suggest a complex set of deltaic wedges, flanked by areas of stagnant sediments, prograded
northward against essentially static shorelines. Detritus
carried by generally northward flowing streams was distributed in a pattern that suggests gradient decreases due to
alluviation, which resulted in constantly shifting depositional loci. Each locus was slightly further seaward of the preceding one. Detrital sedimentation and active chemical
rock deposition appear, in most cases, to have been separated by considerable geographic distance. Active progradation appears to h^ve followed a general shifting pattern
with the major advance toward the north. After major pro
gradation, the clastic wedges commonly went through a cycle
of subsidence, stagnation and transgression all of which was followed by a new episode of detrital influx. Causes of subsidence and transgression were undoubtedly due to a
number of factors, among which compaction of sediments and tectonic forces (perhaps isostatic adjustment) are probably
the most important.
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Zimmerman, R. K., and Ferm, J. C., 1965, Early Allegheny paralic environments in eastern Ohio, Abs.: Southeastern section of the Geological Society of America meeting, Nashville, Tennessee.
Location: Mahoning County, T.19N, R.5W, Section 33, 1.3miles southwest of Sebring in strip mine.
Top of Section:18.0' Sandstone, interbedded siltstone, thickness
estimated2.0 Coal
10.0 Concealed interval, clay exposed at topWater level in strip mine
ALLIANCE #20
Location: Stark County, Lexington Township, Section 36,SE% of SEhi, 0.8 mile east of Mt. Union in clay pit.
Top of Section:34.0' Siltstone and sandstone, interbedded3.0 Concealed interval5.5 Siltstone, thin bedded0.1 Shale, clayey2.0 Coal
Concealed interval, clay exposed at top
77ALLIANCE #21
Location: Mahoning County, Smith Township, Section 19, SE%of NE%, 2.5 miles southeast of Lexington (junction of Courtney and Martin Rds.) in limestone quarry.
Top of Section:
10.0' Till14-16' Limestone
ALLIANCE #22
Location: Mahoning County, Smith Township, Section 18, SE%of NW%, about 0.75 mile southwest of junction of Martin and Middletown Roads in limestone quarry.
Top of Section:
TillLimestone, fossiliferous
ALLIANCE #23
Stark County, Paris Township, Section 12, NE% of NW%, 0.5 mile west of New Franklin in strip mine.
Top of Section:4.0' Shale, silty, buff3.0 Shale, silty, black, sparsely fossiliferous at
top, large 1-2 ' in diameter, limestone concretions
9.7 Shale, silty, grading upward to siltstone, 1 footlayer of sandstone at top
3.0 Shale, black
10.0 '14.3
Location:
78ALLIANCE #24
Locations Stark County, Paris Township, Section 1, NW% of NW%, 0.5 mile west of Georgetown Street and Route 88 junction in strip mine.
Top of Sections15.0' Siltstone and sandstone interbedded, grading up
ward into sandstone, thin bedded, thickness estimated
Location: Stark County, Paris Township, Section 23, NW%of NW%, 0.75 mile northeast of Myers in strip mine.
Top of Section:20.0' Siltstone and shale, interbedded, abundant iron
stone concretions, estimated thickness2.6 Coal (reported by farmer to be under silt and
shale)
ALLIANCE #27
Location: Stark County, Paris Township, Section 9, NE% ofSE% and NE% of NW%, about 1 mile southeast of Paris in strip mine and about 0.5 mile east of Paris in road cut.
Top of Section:10.0' Covered interval (probably sandstone), thickness
33.6 Shale, clayey, dark gray, ironstone concretions,fossils at base, grading upward into shale, brownish yellow, very silty and in turn into siltstone
2.5 Coal, #68.0 Underclay7.0 Sandstone, fine to medium, gray7.0 Siltstone, thinly laminated, thin bedded, mica
ceous, grading upward into fine to medium sandstone
Location: Stark County, Paris Township, Section 25, SE% of NW%, about 0.5 mile west of Highway 183 in Pennsylvania Railroad cut.
Top of Section:15.0 Sandstone, massive, thickness estimated9.7 Shale, very silty, abundant ironstone concre
tions, coal stringers near base
81OHIO
CANTON 15' QUADRANGLE SOURCE OF PLOTTED SECTIONS
Section No. Source1 Geological Survey of Ohio Bull. 28, p. 1322 Geological Survey of Ohio Bull. 49, p. 3143 Ohio Geological Survey file no. 149474 Ohio Geological Survey file no. 149075 Ohio Geological Survey file no. 134846 Ohio Geological Survey file no. 149397 Ohio Geological Survey file no. 149468 Measured and contained in this appendix
82
CANTON #8
Location: Stark County, Lake Township, Section 21, SE%of SW%, about 0.5 mile east of Market Avenue on Midway Street in East Ohio Limestone Company's quarry.
Location: Carroll County, Brown Township, Section 2, SW%of SW%,in abandoned strip mine on east side of road.To fill in above Carrollton #5
Top of Section:
25.0' Covered interval, towards top silty and sandy,about 2/3 up shaly carbonaceous horizon, towards bottom shaly siltstone with occasional 6 "-8 " siltstone lenses
Locations Carroll County, Monroe Township, Section 3, SE%, Section 2, NE%, Section 32, NW% of NW%, on southeast of Ridge Road in abandoned strip mine.
.Top of Section:
Covered IntervalSandstone, channel, interbedded with shale, very
Location: Tuscarawas County, Fairfield Township, Section 8 ,NW% of NE% of NW^, about 0.75 mile west of Somer- dale and 1.5 miles north of Johnston in abandoned strip mine.
Top of Section:151 Sandstone0.5' Coal blossom5 1 Clay0-3' Limestone
28.5' Sandstone, and shale, silty, bedded-51' Shale, clay at bottom becoming silty towards top,
fossiliferous (Washingtonville), (marine zone
91extends 6-7' above coal) limestone concretions and stringers
0.5' Clay? Coal, (Middle Kittanning)
DOVER #68
Location: Stark County, Osnaburg Township, Section 33, SW%of NE%, on north side of road in abandoned strip mine.
Locations Stark County, Sugar Creek Township, Section 33, SW and SE%, about 0.75 mile southeast of Wilmot in strip mine.
Top of Section:? Indefinite covered interval1 1 Clay1* Coal, #6 ?1 1 Clay4' Sandstone, yellowish-brown iron stain, thin-
bedded, cross-bedded 29' Shale, very silty, buff, bedded, becoming gray
with deep iron stain on cleavage planes and sideritic bands, toward the base.
1.5' Coal, #5a?23.5' Clay, slightly silty, light greenish gray, iron
stain becoming grayer toward base and finally dark gray to black and shaly above coal
3.0’ Coal, #5
NAVARRE #27
Location: Tuscarawas County, Franklin Township, about 0.75mile north of School No. 2 in southwest corner of township in strip mine on south side of road.
Top of Section:? Indefinite covered interval2' Coal, 5a?
0.4' Clay, dark gray26' Shale, clayey, grading upward from shale, dark
purplish gray, fissile with iron stain in cleavage planes, and ironstone concretions, to shale, silty clay, with large concentration of ironstone stringers
3.5' Coal, 5?? Covered interval with clay exposed at top
96NAVARRE #28
Locations Stark County, Sugar Creek Township, Section 26, East Central and Section 25, West Central, about1.0 mile north-northeast of Beach City in abandoned strip mine.
Top of Section:? Indefinite covered interval8 ' Sandstone, buff, thin bedded4' Shale, very silty
12' Shale, clayey, grading upward into silty shale,with ironstone concretions
38' Shale grading upward from shale, dark gray, clayfossiliferous, with ironstone concretions, to shale, light gray, clayey ironstone concretions, iron stain on cleavage planes, slightly silty, to shale, greenish yellow, clayey, large ironstone concretions iron stained cleavage planes, slightly silty
2 1 Coal1' Underclay
23' Shale, grading upward from shale, dark gray,clayey, ironstone concretions, fissile, iron stain on cleavage planes, to shale, light gray, very silty, iron stain on cleavage planes
5.5' Covered interval, approximate thickness2' Limestone, fossiliferous, no continuous zone of
limestone was found directly overlying coal, but this position tentatively selected because of greatest number of large loose blocks present at approximately this level in section
? Coal, #4?, exposed at top of covered interval
NAVARRE #29
Location: Tuscarawas County, Dover Township, Section 1, SE%,about 0.75 mile south-southeast of Brandywine School in strip mine.
MILLERSBURG 15' QUADRANGLESOURCE OP PLOTTED SECTIONS
Section No. Source
1 Geological Survey of Ohio Bull. 47, p. 2932 Geological Survey of Ohio Bull. 47, p. 3053 Geological Survey of Ohio Bull. 47, p. 3094 Geological Survey of Ohio Bull. 47, p. 3125 Geological Survey of Ohio Bull. 47, p. 3166 Geological Survey of Ohio Bull. 47, p. 3187 Geological Survey of Ohio Bull. 47, p. 3218 Geological Survey of Ohio Bull. 47, p. 3289 Geological Survey of Ohio Bull. 47, p. 336
UHRICHSVILLE 15' QUADRANGLESOURCE OP PLOTTED SECTIONS
Section No. Source1 Geological Survey of Ohio Bull. 55, pp. 57
& 1012 Geological Survey of Ohio Bull. 55, p. 1203 Geological Survey of Ohio Bull. 55, p. 1204 Geological Survey of Ohio Bull. 55, p. 2145 Geological Survey of Ohio Bull. 55, p. 1776 Geological Survey of Ohio Bull. 55, p. 1767 Geological Survey of Ohio Bull. 55, p. 2108 Geological Survey of Ohio Bull. 55, p. 1809 Geological Survey of Ohio Bull. 55, p. 183
10 Geological Survey of Ohio Bull. 55, p. 18511 Geological Survey of Ohio Bull. 55, p. 19412 Ohio Geological Survey file no. 39113 Ohio Geological Survey file no. 86914 to 18 Measured and contained in this appendix
102UHRX CHSVXLLE #14
Location: Tuscarawas County, Goshen Township, in road cutsouth of bend in Tuscarawas River just south of New Philadelphia.
Top of Section:? Covered interval above to top of hill
38' Sandstone, fine to coarse, buff, thin to mediumbedded, large mica flakes along the bedding planes, all beds cross-bedded (channel sand?) or (levee?), occasional 2-5' shale, silty, clayey, dark gray
23' Siltstone, argillaceous, gray, ("churned"), grading upward after 16 feet to bedded (medium to massive) siltstone, fine to medium grain size
3-4' Coal, Middle Kittanning10' Clay, shaly, dark gray, grading upward into a good
plastic light gray to yellowish underclay 37' Sandstone, fine to very coarse, buff, cross
bedded, (channel sandstone?) in places channeled into underlying coal, (about 5 feet above the bottom is an irregularly channeled- out 0-1 foot coal zone, occasionally with underclay)
31’ Clay, shaly, silty, zone near bottom has coarse,well-rounded sand grains or oolites? in clay matrix, green to dark gray, clay becoming thoroughly bored and mixed towards top (bay clay?), upper 2 feet very plastic, light gray clayey, bored
16’ Limestone, Vanport, slightly silty and argillaceous in thin zones becoming sandy near top and grading into shale above, fossiliferous
23' Shale, dark gray to black, slightly silty but.mostly of clay size, thin zones of limestone concretions, lower 12 feet fossiliferous
2' Limestone, Putnam Hill, dark gray, dense, fossiliferous
0.5-1.O' Shale, dark gray, carbonaceous, grading upward into shaly limestone
10' Shale, sandy and silty, grey, some thin beddingplanes, grading upward into a light gray siltstone which is argillaceous
19' Sandstone, light gray on fresh surface, fine tomedium grain size, micaceous, laminated, crossbedded (channel sandstone?), medium to thick bedding planes, limonite along bedding planes and also large mica flakes
2.0' Coal, variable thickness, sandstone above channeled into coal with occasional thin less than 2 feet of clay directly above coal, the clay (shale) is dark gray with few, less than 6 inches diameter, chert nodules in clay
0-1' Clay, black, carbonaceous, few thin coal layers7' Clay, very silty, dark gray, carbonaceous,
micaceous
UHRICHSVILLE #15
Location: Tuscarawas County, T.7N., R.2W., approximately1 mile northwest of highway 16 and 2 miles northwest of Gnadenhutten in strip mine on west side of road
*
Top of Section:12' Indefinite covered interval comprised of silty
Location: Tuscarawas County, Salem Township, Section 11SW% of NE%, in strip mine 0.75 mile from High ways 36 and 16 at the end of Standard Port Washington town road.
46' Sandstone3' Limestone, cherty, dark gray, fossiliferous,
minimum thickness
COSHOCTON #20
Location; Coshocton County, Jackson Township, about 1 mile southwest of junction of roads 271 and 16, in strip mine and ravine east and west sides of road, respectively.
Top of Section:10 ‘
1.5*8 *4 ’2 '
20 '
36'
Sandstone, buff, medium to coarse grained, lying disconformably over coal, occasional clay lenses between it and coal, clay lenses have dwarfed brachiopods
CoalClay, silty, light greenish to yellow, gray mot
tled, bored and reworked Sandstone, fine grained, very micaceous Shale, sandySandstone and sandy shale, alternating
below it is clayey, slightly silty, has sideritic concretions and occasional limestone stringers
34' Covered interval, probably sandstone171 Covered interval at top coal (3 inches exposed)
underlain by clay (at least 3 feet) silty sandstone at base
5.5' Clay, silty34' Covered interval45' Sandstone
COSHOCTON #21
Location: Coshocton County, Jackson Township, in road cutwest of Route 16, 0.25 mile south of junction of Routes 271 and 16.
Top of Section:3' Limestone, very cherty, fossiliferous, chert in
solid bands and nodular 1.5' Limestone, shaly, dark gray, fossiliferous0.5' Shale, very calcareous, fossiliferous1' Shale, black, very carbonaceous
15.5' Covered interval probably clay3.5' Limestone, dark g:ray to brown, very fossili
ferous
H cm
m
in
113OHIO
BRINKHAVEN 15' QUADRANGLE
Source of Plotted Sections
Section N o . SourceGeological Survey of Ohio Bull. 53, p. 121 Geological Survey of Ohio Bull. 53, p. 149 Ohio Geological Survey file no. 13018 Ohio Geological Survey file no. 4692 Measured and contained in this appendix
114BRINKHAVEN #5
Location: Coshocton County, Bedford Township, Section 7,NE%, along road trending northeast to southwest.
Top of Section:45.5' Covered interval, probably underlain by coal18' Covered interval, clay exposed at top2' Limestone, gray, dense, sparsely fossiliferous4' Covered interval2' Limestone, sandy, fossiliferous6 ’ Covered interval, limestone, sandy, with fossils
in ironstone, exposed at base 931 Covered interval1' Limestone, dark gray, dense, fossiliferous
OHIOCONESVILLE 15' QUADRANGLESOURCE OF PLOTTED SECTIONS
Section No. Source1 Geological Survey of Ohio Bull. 53, p. 702 Geological Survey of Ohio Bull. 53, p. 1933 Geological Survey of Ohio Bull. 53, p. 1614 Ohio Geological Survey file no. 16535 Ohio Geological Survey file no^ 5096 Ohio Geological Survey file no. 5217 to 13 Measured by R. M. Flores
14 to 18 Measured and contained in this appendix
116CONESVILLE #14
Locations Muskingum County, T.2N., R.6W., Section 6 , SW% of SW%, extending from abandoned strip mine to the west along the hill.
Top of Sections ,7 Covered interval, shaly at base, very silty,
tions, fossiliferous just above coal 54' Covered interval at top of which is a coal
(2'?) Middle Kittanning 17' Limestone, cherty
CONESVILLE #16
Locations Muskingum County, Muskingum Township, about 0.7 mile south of Rock Cut in the road cut.
117Top of Section:? Indefinite covered interval concealing uppermost
part of limestone bed below 1.5' Limestone, cherty, dark gray, dense, fossiliferous1' Clay0.3' Coal stringer
10' Clay3.5' Sandstone
28.51 Covered interval containing black flint zone andconcealing bottom part of sandstone above and uppermost part of the light gray, plastic, clay below
2.5' Coal17' Covered interval with partially exposed shale,
silty, grading into siltstone and sandstone and in turn into underclay
Location: Coshocton County, Virginia Township, Section 8 ,SW% of SE j, about 1 mile southwest of church in Willowbrook in Peabody Coal Company's strip mine.
Top of Section:Covered interval Sandstone Siltstone ClayIronstone SandstoneShale, Washingtonville, clay, very fossiliferous,
10 Ohio Geological Survey file no. 71011 Geological Survey of Ohio Bull. 21, p. 15512 >r Ohio Geological Survey file no. 74713 Ohio Geological Survey file no. 40914 Ohio Geological Survey file no. 40715 Ohio Geological Survey file no. 46116 to 18 Measured by R. M. Flores
OHIOPHILO 15' QUADRANGLE
SOURCE OF PLOTTED SECTIONS
Section No. Source
1 Ohio Geological Survey file no. 8262 Ohio Geological Survey file no . 8393 Ohio Geological Survey file no. 5744 Ohio Geological Survey file no. 4755 • Ohio Geological Survey file no. 4816 Ohio Geological Survey file no. 2327 to 12 Measured by R. M. Flores
1 2 1
OHIOZANESVILLE 15' QUADRANGLE
SOURCE OF PLOTTED SECTIONS
Section N o . _ Source
1 Geological Survey of Ohio Bull. 2 1 , p. 1712 Geological Survey of Ohio Bull. 48, p. 1743 Geological Survey of Ohio Bull. 48, p. 1754 Geological Survey of Ohio Bull. 48, p. 2095 Geological Survey of Ohio Bull. 48, p. 2116 Geological Survey of Ohio Bull. 48, p. 2137 Geological Survey of Ohio Bull. 48, p. 2148 Geological Survey of Ohio Bull. 48, p. 2169 Geological Survey of Ohio Bull. 28, p. 129 .
10 Geological Survey of Ohio Bull. 2 1 , p. 14411 Ohio Geological Survey file no. 42012 Ohio Geological Survey file no. 41013 Ohio Geological Survey file no. 46714 Ohio Geological Survey file no. 78815 Geological Survey of Ohio Bull. 2 1 , p. 13116 Geological Survey of Ohio Bull. 2 1 , p. 14017 Ohio Geological Survey file no. 34818 Ohio Geological Survey file no. 38219 Ohio Geological Survey file ho. 1095520 Ohio Geological Survey file no. 850821 Ohio Geological Survey file no. 77222 Ohio Geological Survey file no. 76923 Ohio Geological Survey file no. 77324 to 36 Measured by R. M. Flores37 Measured and contained in this appendix
1 2 2
ZANESVILLE #37
Location: Muskingum County, T.1N., R.8W., in Zanesvillealong road cut 100 yards east of Licking River on north side of road.
Top of Section:8 ' Covered interval, probably shaly siltstone8 ' Covered interval with silty shale2.5' Limestone, Putnam Hill, fossiliferous0.7' Shale
10' Siltstone, dark gray, shaly1' Shale, black1.5' Coal
VITA
Ronald K. Zimmerman was born in Wabash County, Illinois
on January 6 # 1935. He attended public primary and secondary schools in that county, graduating from Mt. Carmel High
School in the spring of 1952. He completed a tour of duty
with the United States Army in December of 1956. In September, 1957 he entered Augustana College at Rock Island, Illinois, transferred to the University of Illinois in
September, 1958, and was granted a Bachelor of Science degree
from that institution in August of 1960.He entered the graduate school at Louisiana State Uni
versity in September, 1960 and received a Master of Science degree in geology in June, 1963. While studying at Louisi
ana State University, he held an industrial fellowship with
Coastal Studies Institute from February, 1961 to June,1962, a graduate assistantship in the Department of Geology
during the academic years of 1962-63 and 1963-64, and the Socony Mobil Oil Company Fellowship in geology during the academic year 1964-65.
123
He is a member of the Society of Sigma Xi and American
Association of Petroleum Geologists. He has been employed as a geologist in the exploration department of Humble Oil
and Refining Company since August 1965.
EXAMINATION AND THESIS REPORT
Candidate:
Major Field:
Title of Thesis:
Ronald K. Zimmerman
Geology
Aspects of Early Allegheny Depositional Environments in Eastern Ohio
Approved:
Professor ana Chairman
Dean of the Graduate School
EXAMINING COMMITTEE:
Date of Examination:
May 5, 1966
LOCATION OF STRATIGRAI
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EXPLANATION
15’ QUADRANGLE IDENTIFICATION
A Alliance • LV LoudonvilleAT Athens M MillersburgBV Beaver N NavarreB Bri'nkhaven NL New LexingtonCZ Cadiz - NW NewcastleCN Canton NC NewcomerstownCT Carrollton P PhiloC Columbiana SL SalinevilleCV Conesville SC ScioCS ; Coshocton SB SteubenvilleD Dover U UhrichsvilleF Frazeysburg w We11svilieJ Jackson WK WilkesvilleLR Laurelville Z ZaleskiL Lisbon ZV ZanesvilleLG Logan
N 12 Location of plotted section by quadrangle
40°00'
is Location of cross sections shown in
39°30'
39°00'
iO£ol8 i00o38
N 151 QUADRANGLE IDENTIFICATION
A Alliance LV LoudonvilieAT Athens M MillersburgBV Beaver N NavarreB Brinkhaven NL New LexingtonCZ Cadiz NW NewcastleCN Canton NC NewcomerstownCT Carrollton P ..PhiloC Columbiana SL SalinevilleCV Conesville SC ScioCS Coshocton SB SteubenvilleD Dover U UhrichsvilleF Frazeysburg W We11svilieJ Jackson WK WilkesvilleLR Laurelville Z ZaleskiL Lisbon ZV ZanesvilleLG Logan
. 12 Location of plotted section by quadrangle
8 Location of cross sections shown in 10 15............................. ...■ ■ ■ K = = ) ** •ILES plates II through VI.
MARINE - BRACKISH LIMESTONE, BEDS, LENSES, a NODULES
FRESH-WATER LIMESTONE LENSES
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CHEMICAL ROCKS DETRITAL ROCKS, 1,1,1,. M A R I N E - B R A C K I S H L IM E S T O N E ,
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COAL
"SEATROCK "(UND ERCLAY )
SIL T ST O N E 8 SILTY SH /
CLAY SH A L E
F E E T — 80
— 60
— 40
O
SYMBOLS
D 33
\ 7
MARINE - BRACKISH F O S S IL S
BRACKISH F O S S I L S
CONTACT, A B R U PT 8 GRADATIONAL
STRATIGRAPHIC SE C T IO N 8 NUMBER
COVERED INTERVAL
CROSS SECTION A -BSEE PLATE I FOR GEOGRAPHIC LOCATION
9 /» O >f /•
COSHOCTON | ML
URG NAVARR R
M IDDLE KITTANNING 6
NAVARRE
N 26 II CJN 28
V‘KI!-:,'
MIDDLE KITTANNING 6
CHEMICAL ROCKSM ARIN E-BRA CK ISH L L E N S E S , A NODULE
F WFR E SH -W A T E R LIME:
EXPLANATION
MICAL ROCKSH M A R IN E -B R A C K IS H L IM E S T O N E , BEDS, J L E N S E S , a N O D U LES
]> F R E S H -W A T E R LIM ESTO N E L E N S E S
DETRITAL ROCKS
SA N D STO N E
SILTSTONE & SILTY SHALE
A
CS9
VANPORT-
•PUTNAM HILL
f cU3T >DC
U$ /
-V /
-BROOKVILLE ” 4
LOWERKITTANNING
N 2 8 MIDDLE KITTANNING ~ 6
SCARAWAS.T. r i _
RASBURGSo
N 2 3
COLUMBIANA ~ -_r-
V
D 6 6is:D 6 5
7\
•'i-
LOWERKITTANNING
ISri lF *
IM l!l lEil LIJ Ed
F W
<£> <*>
<X>
7 X t ?\ 77
FR E S H -W A T E R LIMESTONE LEN SES
CHERT, BEDS a NODULES
IRONSTONE, LAYERS 6 NODULES
COAL
"SEATROCK"(UNDERCLAY)
SILTSTONE 8 SILTY SHALE
CLAY SHALE
F E E T
-80
— 60
— 40
— 2 0
SYMBOLS
D 3 3
MARINE - BRACKISH FOSSILS
BRACKISH FOSSILS
CONTACT, ABRUPT a GRADATIONAL
STRATIGRAPHIC SECTION 8 NUMBER
COVERED INTERVAL
CROSS SECTION C -DSEE PLATE I FOR GEOGRAPHIC LOCATION
NAVARR. DOVER
Ftf?EDO
V£
K
UHHJCHSVJLL
U 14 J.
NAYAR
'A a p £
D0
V
£
R
UHRJCHSVJi F!
U 14 J.
'tit
CHE*
EXPLANATION
CHEMICAL ROCKS DETRITAL ROCKSMARINE - BRACKISH LIM ESTONE, BEDS, SANDSTONEL E N S E S , 8 NODULES ::l\;hv=;
FR E SH -W A T E R LIM ESTONE L E N S E S s il t s t o n e a
28 n 32* * *•
M ID D L E K IT T A N N IN G
¥STRASBURG 5 a
LOW ER KITTANNING 5
N 16
COLUM BIANA
r x * PU TN A M
i t ? HILL
B R O O K V IL L E 4
V A N P O R T
TUSCARAWAS
I 18M IO O LE K IT T A N N IN G 6
N 31 yS T R A S B U R G * 5 a
J-- M -
-)
- - CO LU M B IA N A
L O W E R K ITTA N N IN G 5
VAN P O R T
M H IL L
TUSCARAWAS
FW
18M IDDLE K ITTA N N IN G 6
N 31- - / S T R A S B U R G - 5 a
*■?i i --)
COLUMBIANA3
LOWER KITTANNING 5
VAN P O R T
HILL
□
- "ajssr
A (L.<3? <5>
<s>
Y S
— £ 0
\& | LENSES, ft NODULES
F W
-A A.<37 <S>
FR E SH -W A T E R LIMESTONE L E N S E S
CHERT, BEDS 8 NODULES
Isl'iiUil*.:! SANDSTONE
SILTSTO N E 8 SILTY SHALE
CLAY SH ALE
333EZT*S> <S> IRONSTONE, LAYERS 8 NODULES
COAL o
v s "SEA T R O C K " (UNDERCLAY)
F E E T r-eo
60
— 40
—20
SYMBOLS
-car
£
D 3 3 -X.-
MARINE - BRACKISH FO SSILS
BRACKISH FO SSILS
CONTACT, ABRUPT 8 GRADATIONAL
STRATIGRAPHIC SECTION 8 NUMBER
COVERED INTERVAL
CROSS SECTION E -F 8 G-JSEE P L A T E I FOR GEOGRAPHIC LOCATION
MILLERSBURG NAVARRE
N 12
LOWER
COSHOCTON
K.
/
L O W E R F R E E P O R T
COSHOCTON
OjVJEHSTOVVN
I
UHRJCHSVJL1 o v .
H / /
S C 2
U 6
U P P E R F R E E P O R T
U 18 L O W E R F R E E P O R T ,
XR U N
$v/.:
* * •
•*\¥ '
t o
'OWN
✓JL P.
H
UPPER FREEPORT
U 18Y■\4
■U'.l
.* ".v.tFW<^Z=s>
*«»♦
£
LOWER FREEPORT.
CHEMIC7 = P = t | M<£> LI
EXPLANATION
CHEMICAL ROCKS DETRITAL ROCKSMARINE - BRACKISH L I M E S T O N E , BEDS,L E N S E S , a N O D U L E S , . * •* St *#
<r'r iTS F R E S H - W A T E R 1T T -1 .
S A N D S T O N E
S I L T S T O N E a SILTY S H A L E
"MIDDLE KITTANNING 6
, WASHINGTONVILLE
COLUMBIANA
N 14
LOWER KITTA N N IN G *!
N 13
*
V
PUTNAM HI
' - 'BROOKVILLE * 4
N 29
I ING ^ 5
n
%JL L l L j ^ VAN p o r t
1AM H I L L ^ -
T—- r 1-
■±'&r
• r —• “ - TfSr
* 4
CS 9r ? ?17
/
0 3 ON
ak*6 SO
V j$ T :6 ON1—1|
\£i-tL
NC 14
BROOKVILLE 4
LOWER KITTANNING 5
- - - \
^WASHINGTON VILLE
MIDDLE KITTANNING ^ 6
‘Stt ^ -C O L U M B IA N A
i
PUTNAM HILL
N 6 T 0 N V I L L E
K I T T A N N I N G 6
L U M B IA N A
ING * 5
NC 14
ft\
-***
E*4
.JL•••ih C'“
U5
WASHINGTON VILLE
MIDDLE KITTANNING ^ 6
'SrSr ^ —-COLUMBIANA
. «
.“IittCS
LOWER KITTANNING 5
PUTNAM HILL
Ul
|<& l e n s e s , a NODUL
<8? ®
FRESH-WATER
CHERT, BEDS 8 1
IRONSTONE, LAYEf
COAL
"SEATROCK" (UNDEI
F E E T SYIVr-80
*€5
h -60
t - 40 -RT5V A
I— 2 0
L - O
CROSS
|<& ^ | L E N S E S , f t N O D U LES
F R E S H - W A T E R
<XS> <s>
<s> «>
CHERT, BEDS 8 N O D U L E S
I R O N S T O N E , L A Y E R S 8 NO DULES
COAL
" S E A T R O C K " (U N D E R C L A Y )
K I SANDSTONE I: 1
SILTSTONE 8 SILTY SHALE
CLAY SHALE
FEET — 80
— 60
— 40
— 2 0
*— 0
SYMBOLS
" O ’
D 3 3
V
MARINE - BRACKISH F O S S I L S
BRACKISH FOSSILS
CONTACT, A B R U P T 8 GRADATIONAL
STRATIGRAPHIC SECTION 8 NUMBER
COVERED INTERVAL
CROSS SECTION l-J -H 8 K-H-MS E E P L A T E I FOR GEOGRAPHIC LOCATION
2 0 2 4 6
COSHOCTON
MIDDLE KITTANNING * 6
jNEVVCOjVJERSTo w n
L.
NC 23 NC 3
EXPLANATION
CHEMICAL ROCKS DE‘r*.i±iJLi M ARINE-BRACKISH LIMESTONE,
BEDS, LENSES, a NODULES. u .»•’ l*.» •*
nr* FRESH-WATER LIMESTONE LENSES . —JJ.
E X P L A N A T I O N
ICAL ROCKS DETRITAL ROCKSM A R IN E -B R A C K IS H L IM E ST O N E , BEDS, L E N S E S , a NODULES
|.l. L. 1.1. TP..a
•• l* • ' SANDSTONE
F R E S H -W A T E R LIMESTONE LENSES I v - f l SILTSTONE a SILTY SHALE
CS 3
MIDDLE KITTANNING 6
LOWER KITTANNING 5
- — *
PUTNAM HILL
BROOKVILLE
|€> ^ I BEDS, LENSES, 8 NODULES li” *i ~ v I -i
'sr.sr.
333CC ® 9
*1
FR ESH-W ATER LIMESTONE LENSES
CHERT, BEDS 8 N O D U L E S
IRONSTONE, LAYERS 8 NODULES
COAL
"SEATROCK"(UNDERCLAY)
SI
F E E T
r-80
60
— 40
— 2 0
^ - 0
SYMBOLS
D 3 3
V
MARINE-BRACKISH FOSSIL!
BRACKISH FOSSILS
CONTACT, ABRUPT 8 GRAI
STRATI GRAPHIC SECTION
COVERED INTERVAL
CROSS SECTION (SEE P L A T E I FOR GEOGRAPHIC
2 O 2 4
BEDS, LENSES, a NODULES F“,v I li”*i ~ v i -I
FRESH-W ATER LIMESTONE LENSES
CHERT, BEDS 8 N O D U L E S
SILTSTONE 8 SILTY SHALE
CLAY SHALE
«T IRONSTONE, LAYERS 8 NODULES
COAL
V f "SEATROCK"(UNDERCLAY)
SYMBOLS
D 3 3
VA
MARINE-BRACKISH FOSSILS
BRACKISH FOSSILS
CONTACT, ABRUPT 8 GRADATIONAL
STRATI GRAPHIC SECTION 8 NUMBER
COVERED INTERVAL
CROSS SECTION C -LSEE P L A T E I FOR GEOGRAPHIC LOCATION