Vertical variability and lateral distribution of late Wisconsinan sediments parallel to the axis of the buried valley of Mud Brook North of Akron, Summit County, Ohio.
Szabo, John P. ; Huth-Pyscher, Christine G. ; Kushner, Vaughn A. 等
ABSTRACT: The buried valley of Mud Brook in northern Summit County,
OH, contains sediments associated with the late Wisconsinan glaciation.
The vertical variability and lateral distribution of these sediments can
be ascertained from information derived from logs from highway borings
and water wells along a 15-km north-south transect parallel to the axis
of the buried valley. Textural, carbonate, clay mineral, and lithologic
analyses of samples from roadcuts, geological borings, and some highway
department borings provide additional information to assign lithofacies
units to specific glaciations. Cross sections show that nearly similar
depositional environments existed before each late Wisconsinan glacial
advance. The proglacial sediments consist of outwash and lacustrine
deposits overridden by ice that deposited an overlying till. Sediments
associated with the Lavery and Hiram advances overlie a Kent-aged kame
plateau within the Summit County Morainic Complex at the southern end of
the study area. Farther north meltwater accumulated and drowned ground
moraine to form post-glacial lakes that were eventually drained as the
drainage network of Mud Brook became better integrated.
Date of publication: January 2013
INTRODUCTION
The deposits in the buried valleys of the glaciated northern
Allegheny Plateaus may contain a record of several glacial advances
during the Pleistocene epoch. Several of these valleys such as that of
the lower Cuyahoga River in northern Ohio are being exhumed by modern
rivers; tributaries of these rivers dissect the valley fill exposing
sediments that represent processes associated with glaciation (Szabo
1987, 2006a). Other buried valleys remain completely filled and may be
poorly drained by low-gradient, sluggish streams flowing across old
lakebeds and through wetlands (Ohio Drilling Co. 1971), Mud Brook in
northern Summit County, OH (Fig. 1), is an example of the latter where
the glacial stratigraphy can only be determined by the use of subsurface
data.
The buried valley beneath Mud Brook is located five km east of that
of the lower Cuyahoga Valley. The local glacial stratigraphy and
proximity of these two large bedrock valleys suggest that master streams
may not have occupied both valleys at the same time (Szabo, 2006a). The
occurrence of late Wisconsinan tills on interfluves of streams
dissecting the valley fill of the Cuyahoga River valley may imply that
it was completely filled prior to the late Wisconsinan glaciation.
Kushner (2006) has inferred that the valley of Mud Brook may have been
incised to bedrock prior to late Wisconsinan advance based on the
presence of deeply weathered Orangeville shale found in borings into the
valley bottom. Additionally, farther to the south Wilson (1991) found
thick sequences of late Wisconsinan sediments. The purpose of this study
is to examine the vertical variability and distribution of late
Wisconsinan sediments in a north-south direction parallel to the axis of
the buried valley of Mud Brook.
The bedrock geology and glacial geology of the study area are
variable. The buried valley of Mud Brook (Fig. 2) begins near State
Route 82 in northern Summit County (Smith and White 1953, Schmidt 1979)
where it is incised into siltstones and shales of the Mississippian
Cuyahoga Formation. The bedrock valley floor descends at the rate of six
m/km and is eroded into Devonian shales in the southwest corner of the
study area (Fig. 2). Sandstones and conglomerates of the Pennsylvanian
Sharon Formation underlie the adjacent uplands (Fig. 3). A seismic
investigation (Gardner 1981) of the buried valley south of Steeles
Corners Road (Fig. 2) suggests that the valley may be deeper than
indicated on the generalize d map (Fig. 2). A resistivity survey
centered on the area bounded by the 700-foot bedrock contour north of
Steeles Corners Road (Fig. 2) determined that the fill of the buried
valley was dominated by clay with layers or lenses of silt, sand, and
sand and gravel (Olver 1981).
The area was affected by several Pleistocene glaciations. Illinoian
deltaic and lacustrine sediments up to 40 m thick and tills are found in
valleys of tributaries to the Cuyahoga Valley to the west (Ryan 1980,
Szabo and Ryan 1980, Szabo 1987) and are associated with the ice
advances that deposited the Millbrook and Northampton tills (Table 1).
The late Wisconsinan Kent, Lavery, and Hiram tills (Table 1) are well
represented in the study area (Ryan 1980, Wilson 1991, Kushner 2006) but
may be absent in parts of the adjacent Cuyahoga Valley.
[FIGURE 1 OMITTED]
[FIGURE 2 OMITTED]
The topography of the lowland over the buried valley consists of
gently rolling knolls of till surrounded by nearly flat areas occupied
by wetlands and former lakebeds. The topography near Steeles Corners and
Graham roads in the southern part of the study area (Fig. 3) consists of
moraine and ice-contact deposits of the Summit County Morainic Complex
(White 1982, 1984). The morainic complex is a superposed moraine having
its bulk composed of Illinoian Northampton Till with successive layers
of Lavery and Hiram tills draped over it (Ryan 1980). A large lakebed
extends northward from the Complex to elements of the Defiance Moraine
to the west (Pavey and others, 1999). Mud Brook originates in this
lakebed and flows southward through wetlands within the morainic complex
before turning westward (Fig. 3) to eventually join the Cuyahoga River.
Allahiari (1983) performed a morphometric analysis of the Mud Brook
basin and showed that there were differences between tributaries of Mud
Brook that drain the area over the buried valley and those that drained
the valley fill of the Cuyahoga Valley southwest of the study area.
Downcutting by upper Mud Brook is limited by a sandstone knickpoint near
the intersection of State Route 8 and Graham Road in the southwestern
part of the study area (Fig. 2). Upstream of the knickpoint the
tributary basins to Mud Brook have long first-order streams, low mean
channel slopes, and low basin reliefs, whereas those downstream of the
knickpoint have high mean channel slopes, high basin reliefs, and large
stream frequencies and drainage densities (Allahiari 1983). These
tributaries are closer to the Cuyahoga River, which is the base level
for lower Mud Brook.
[FIGURE 3 OMITTED]
The deep dissection of the lower Cuyahoga valley and its
tributaries provides numerous outcrops from which the glacial
stratigraphy can be determined (Szabo 1987). However the extent of the
units exposed in this valley cannot be traced eastward without the use
of subsurface data. This study uses the acquisition and interpretation
of subsurface data and the laboratory analyses of surface and subsurface
samples to trace late Wisconsinan units into the upland east of the
Cuyahoga valley and to improve on the interpretation of their
environments of deposition.
MATERIALS AND METHODS
Data used in this study were collected from borehole logs and
samples from URS Corporation, roadcuts and additional borings by the
authors (Wilson 1991, Kushner 2006), borehole descriptions for new State
Route 8 from the Ohio Department of Transportation (ODOT), and
water-well logs. URS supplied borehole logs and 147 samples for ten deep
borings (Kushner 2006). Eleven grassed road cuts were sampled at one-m
intervals using a horizontally driven core sampler, and 13 boreholes
were drilled at the base of the cuts and at other locations using a
Giddings soil probe. These provided an additional 288 samples (Wilson
1991). Also borehole logs from 27 additional ODOT borings and well logs
of 15 water wells were examined to improve correlations among the other
subsurface data.
Samples from these various sources were examined, and their Munsell
color, texture, consistency, structure, and reaction to dilute HCl were
noted. In the laboratory, matrix textures (% < 2 ram) were determined
using a settling and pipetting methods modified from Folk (1974). The
sand-silt break in this study is 0.063 mm and the silt-clay break is 4.0
[mu]. The fine-carbonate content (% < 0.074 ram) was determined using
a Chittick apparatus (Dreimanis 1962). This size range is the terminal
grade for calcite and dolomite and can be related to the provenance of
the glacial deposits. The terminal grade is the smallest size to which a
rock fragment may be crushed or abraded given the available energy in a
glacial environment. Diffraction intensity ratios (DIs) of the clay
fractions (<2.0 [mu]) of some samples (Kushner, 2006) were calculated
by measuring the area under the illite peak at 1.0 nm and dividing it by
the area under the combined kaolinite and chlorite peak at 0.7 nm
(Willman and others 1966, Bruno and others 2006). The lithology of the
one to two mm fraction was determined for some samples (Wilson 1991)
using a binocular microscope because this fraction is representative of
the pebble contents of tills (Anderson 1957). Rock fragment data derived
from this procedure were combined to form three categories: elastics,
carbonates, and crytallines (Table 2).
Laboratory data, sample descriptions, and borehole logs were used
to differentiate among various glacial sediments (Table 2) including
those deposited by direct melting of the ice (diamict or till), those
deposited by meltwater (silt, sand, and gravel), and those deposited in
glacial lakes (clay). Additionally carbonate content was used to assign
samples to a particular glacial advance using data summarized in Szabo
(2006b). Descriptive statistics were calculated for each lithologic unit
(Table 2). North-south geologic cross sections (Fig. 2) showing the age
assignments for various groups of units were prepared using the borehole
data. Additionally, more detailed cross sections illustrating the
geometry of the various lithologic units were drawn for the northern
traverse A-A' and the most southernmost two km of traverse
C-C' (Fig. 2).
RESULTS
The samples from the borings were grouped into different
lithofacies based on grain size and include: interbedded sand, silt, and
clay; interbedded silt and clay; silt; sand; sand and gravel; and
diamict. We use the term, diamict, for unsorted mixtures of sediment
ranging from clay to gravel. Diamicts may have a variety of origins, but
in this paper we interpret that they originated in a glacial environment
and thus can be referred to as tills when discussing the glacial history
of the area. Fine-grained units dominate the subsurface in the northern
part of the study area (Kushner 2006), whereas sand and gravel is more
common in the southern part (Wilson 1991). Lithofacies were grouped into
age units representing different ice advances using stratigraphy from
the boreholes and fine-carbonate contents. Similar lithofacies among age
units were compared statistically using t tests at P [is less than or
equal to] 0.05 (Kushner 2006, Wilson 1991) verifying that the separation
by fine-carbonate contents was valid.
Cross Section A-A'
Cross section A-A' (Fig. 4) is constructed from data from ten
boreholes of which, eight extended into shale. The deep borings
terminate in dark gray, fissile shale that correlates with the
Mississippian Orangeville Shale Member of the Cuyahoga Formation. Sand
and gravel overlies the shale in the center of the cross section (Fig.
4) and has a bipartite nature. The lower part of the sand and gravel
contains abundant shale fragments; X-ray diffractograms of the shale
show that illite has degraded suggesting that weathered shale was
incorporated into the gravels (Kushner 2006). The upper part of the gray
gravel has calcite and dolomite contents similar to those of overlying
Lavery lithofacies (Table 2). Gray, fine-grained deposits ranging from
three to 20 m in thickness overlie the shale and sand and gravel (Fig.
4) and have fine-carbonate contents associated with those of the Lavery
Till (Szabo 2006a). Their average DIs (Table 2) represent the erosion
and comminution of lower Paleozoic shales by ice (Szabo and Fernandez
1984, Szabo 2006a). Gray, firm, Lavery diamict overlies the fine-grained
units, is from two to six m thick, and is discontinuous across the
length of the cross section as it rises in elevation southward (Fig. 4).
The texture of the Lavery diamict is less clayey than that found just
west of the study area in Northampton Township (Ryan 1980), but less
silty than that found in southern part of the study area (Wilson 1991).
Its total fine carbonate is somewhat less than those values found in
other studies in Summit County (Ryan 1980, Angle 1982, Wilson 1991). The
average DI of the diamict is 1.5 and is similar to that of the local
Mississippian bedrock (Szabo and Fernandez 1984).
Massive to laminated, firm fine-grained lithofacies dominate
deposits associated with the Hiram advance and range from two to 17 m
thick (Fig. 4). These lithofacies are weathered brown to gray brown near
the surface and become grayer with depth. Where at the surface, these
units are leached of fine carbonates and their DIs may be as large as
4.0, suggestive of the weathering of chlorite. Within the interbedded
silt and clay, calcite contents are significantly larger than dolomite
contents (Table 2). In the southernmost borehole (SB 101, Fig. 4), 1.5 m
of very firm, weakly calcareous diamict overlies gray, calcareous
interbedded silt and clay. This is the only occurrence of Hiram Till
within the length of the cross section.
Cross Section B-B'
The 1.2-km longcross section B-B' (Fig. 5) is an attempt to
trace the sedimentary units farther south by using nine water-well logs
from the Ohio Division of Water. This cross section is parallel to the
axis of buried valley and uses data from water wells as deep as 32 m
along Wakers Road (Fig. 2). The superficial descriptions of sediments by
various well drillers make it difficult to differentiate among units. We
interpret "clay with stones" or "clay with gravel"
to be diamicts and "clay with sand" as interbedded units. We
are able to separate the sediments recorded in the well logs into
deposits of two ages using the occurrence of diamicts in the wells, our
interpretation of cross section A-A', and the occurrence of a
diamict on the surface (Fig. 3). Hiram-age deposits include the
surficial till and fine-grained sediments. Because the Lavery diamict
overlies other Lavery-age deposits, we placed the contact between Hiram-
and Lavery-age sediments at the top of the second diamict recorded in
the well logs.
Cross Section C-C'
Cross section C-C' extends nine km between State Route 303 and
Graham Road in Stow where it ends in the Summit County Morainic Complex
(Fig. 2). Data for construction of the cross section come from 18 ODOT
borings, 12 borings using a Giddings soil probe, 11 measured sections,
and six water wells (Fig. 6) collected by Wilson (1991). Her study also
incorporates data from four boreholes and three outcrops not along the
line of the cross section. This cross section illustrates the
distribution of sediments associated with three late Wisconsinan
advances, possible older deposits at depth below the southern part of
the study area, and the occurrence of resistant sandstone topographic
highs (Fig. 6). Kent sediments are relatively continuous across the
length of the cross section, whereas Lavery deposits are somewhat less
continuous, and Hiram diamicts are relatively discontinuous in
comparison (Fig. 6).
There are three lithofacies associated with the Kent advance
(Wilson 1991). Friable to firm, silty diamicts are olive brown where
oxidized and dark olive gray where unweathered. They contain granules
and pebbles and have a slightly delayed reaction to HC1 reflective of
their small fine-carbonate contents dominated by dolomite (Table 2).
Their one to two mm sand fractions contain an average of 13 percent
carbonate and are dominated by local sandstone, siltstone, and shale
clasts. Silts associated with the Kent advance are massive and firm and
weather olive brown. Gray unweathered silts contain an average of 1.1
percent calcite and 4.6 percent dolomite (Table 2); isolated sand layers
within the silt contain an average of 21 percent carbonate, which is
significantly larger than comparable values for diamicts and sands. Kent
sands are generally friable, well sorted, and quartzose. The matrix
textures of the Kent sands are silty (Table 2) and contain very little
clay. Near-surface sands oxidize brown and are leached of carbonates,
whereas deeper sands are olive brown and average about 5.5 percent fine
carbonates again dominated by dolomite. The average composition of their
sand lithologies is similar to that of the diamict.
[FIGURE 4 OMITTED]
Diamict and sand are the only two lithofacies representing the
Lavery advance. Very firm, dark brown, oxidized Lavery diamicts have a
very strong reaction to HC1 and contain secondary carbonates deposited
along fractures within the diamicts or as nodules on weathered surfaces.
Unoxidized diamicts are dark gray with olive or brown mottling. Fine
carbonates consist of nearly equal proportions of calcite and dolomite
and average almost nine percent total carbonate. The average one to two
mm sand lithology of the diamict is similar to that of the Kent sand
(Table 2). Friable, olive gray Lavery sand has an average matrix texture
containingless sand and more clay than that of the Kent sand. The
fine-carbonate content of the sand averages 11 percent and is larger
than that of the diamict. However, its dolomite content is much larger
than its calcite content (Table 2). The one to two mm sand fractions of
this lithofacies contain more crystalline rock fragments than any other
lithofacies illustrated in this cross section.
The Hiram advance is represented by yellowish-brown, friable,
oxidized diamicts containing granules and small pebbles. These diamicts
have a moderate to strong reaction with HCl, but contain no secondary
carbonates. Fifty-five percent of the Hiram samples contained fine
carbonate; samples average 12.6 percent total fine carbonate and in
contrast to other sediments found along the cross section, contain
significantly more calcite than dolomite (Table 2). The coarse sand
lithologies are similar to those of other lithofacies found in the area.
Wilson (1991) included a diagram showing the various lithofacies
along cross section C-C'. The general geometry of the deposits can
be demonstrated by examining the relationships among lithofacies along
the southernmost third of cross section C-C' (Fig. 7) that extends
two km northward from Graham Road (Fig. 2). The various sources of
subsurface data suggest that there are at least 30 m of sediment
overlying shale at the southern end of the cross section: the bulk of
this sediment may be pre-Kent in age. Although predominantly sand (Fig.
7), silt, sand and gravel, and diamicts are also present in the
subsurface. Kent-aged deposits occur close to the surface and consist of
extensive silt and sand overlain by diamict. Multiple Kent diamicts
separated by sand form one of the hills (Fig. 7), and Lavery diamicts
cap most hilltops. Hiram diamict is only present in the southernmost
part of Figure 7 where it overlies Lavery sand and Kent diamict. Cross
sections A-A' (Fig. 5) and C- C' (Fig. 7) show that diamict is
the last material deposited at the end of each glacial advance.
DISCUSSION
This study illustrates several aspects of glacial deposition over
former buried valleys. One of these is that the modern drainage may or
may not follow the buried valley. When examining the distribution of
buried valleys, it becomes apparent that not all valleys can be combined
to form an integrated drainage system (Szabo 2006a). Some ancient
valleys are deeply incised into bedrock well below any modern base
level. The bottom of the buried valley of the Cuyahoga River near
Cleveland is almost at sea level (Szabo 1987), and yet the modern
Cuyahoga River enters Lake Erie at 173 m above sea level. Just west of
the study area bedrock is about 150 m below the flood plain of the
Cuyahoga River (Mangun and others 1981). The bedrock valley floor of Mud
Brook in the southwestern part of the study area (Fig. 2) is about 150 m
below the surrounding upland and is tied into the ancient valley of the
Cuyahoga River.
[FIGURE 5 OMITTED]
A tributary to the Mudbrook buried valley flowed northwestward from
the southeastern corner of the study area (Fig. 2), but it is evident
that glacial meltwater flowed southeastward at State Route 59 (Fig. 3)
as suggested by the distribution of sand and gravel confined by bedrock,
presence of kettle lakes in the meltwater channel, and thick deposits of
sand (Fig. 7). This outwash train continues southward through Akron,
eventually joining the Tuscarawas River (Szabo 2006a). The modern course
of Mud Brook has returned to follow its ancestral drainage to the
southwest (Fig. 3) having formed as a consequence of the post-glacial
topography and headward erosion of a post-glacial tributary following
the buried valley of Mud Brook from the Cuyahoga Valley.
Another important aspect of this buried valley is that it
illustrates the occurrence of similar depositional processes for each
ice advance. There may have been an extensive ice-flee period between
the end of the Illinoian glaciations that deposited the Mogadore and
Northampton tills (Table 1). The sequence of thick sediments well below
the Kent-aged deposits in the southern part of the study area may be
Illinoian in age (Fig. 7). The presence of intensely weathered shale in
the lower part of the basal sand and gravel (Fig. 4) suggests a period
of weathering and fluvial erosion during the Sangamonian Interglaciation
and before the late Wisconsinan advances (Kushner 2006).
[FIGURE 6 OMITTED]
Kent ice advanced southward out of the Erie basin about 23,000
radiocarbon years ago (Szabo 2006a). Wilson (1991) suspected that the
Kent ice of the Grand River lobe may have flowed into the study area
from the northeast. Her hypothesis is based on the absence of Kent
deposits west of the study area (Ryan 1980) and only as far south as
Garfield Heights north of the study area (Szabo 2006a). Thus the study
area may have been an ice-marginal area accounting for the majority of
silty water-laid deposits (Fig. 7) that were reworked into Kent-age
deposits. Topographically the hills in the ice-contact area (Fig. 3)
appear to be kames, but their internal structure reflects a slightly
different mode of origin. The distribution of sediments in the area and
the generally flat-topped nature of the kames not apparent on the
vertically exaggerated cross sections suggest that the ice-contact area
may have originated as a kame plateau (Brodzikowski and Van Loon 1987)
consisting of small lakes and meltwater stream channels initially
forming on top of the ice and let down on the landscape as the ice
melted. The presence of Kent diamicts in the upper parts of the kames
may imply local readvance during a prolonged period of stagnation of
Kent ice on the Allegheny Plateau (Szabo 2006a).
[FIGURE 7 OMITTED]
After retreat of the Kent ice margin into Canada during the Erie
Interstade about 16,500 radiocarbon years ago (Szabo 2006a), an ancestor
of Mud Brook may have continued to drain the area. The northern cross
section, A-A' (Fig. 4) may suggest this or proglacial meltwater
from the first advance after the interstade may have removed any
Kent-aged deposits in the area. Heavy-mineral assemblages in tills
deposited just after the Erie Interstade suggest a major change in ice
flow from north-south across the Erie Basin to northeast-southwest down
the axis of modern Lake Erie (Hofer and Szabo 1993). As Lavery ice from
the Cuyahoga lobe (Szabo 2006a) advanced southward through the study
area, proglacial meltwater may have removed any older Kent deposits
depositing abundant fine-grained sediments and sand and gravel (Fig. 4).
Slight increases in Dis and mottling of laminated clays suggest a
possible in washing of weathered sediments from local topographic highs.
Lavery ice advanced over its own proglacial sediments until it reached
the Summit County Morainic complex north of the modern Cuyahoga River.
There it augmented the bulk of the original moraine and kame plateau by
superposing a layer of diamict over the older deposits. The maximum
extent of Lavery ice appears to have been just south of Graham Road
(Fig. 3).
Following a retreat of Lavery ice northward into the Erie basin,
Hiram ice flowed southward depositing a similar depositional sequence as
that deposited by the Lavery ice (Fig. 4). Again fine-grained sediments
were deposited proglacially and overridden by Hiram ice that laid down a
layer of diamict as it advanced to the morainic complex. The relief of
the area was again increased by the addition of another layer of
superposed diamict (Fig. 7). Meltwater may have been directed along the
margin of the ice at this time to form the middle Cuyahoga River that
drained through a sag in what is now downtown Akron into the Tuscarawas
River. It is not known if the ice masses that eventually formed the
kettle lakes at the margin of the morainic complex broke off from Lavery
or Hiram ice. However, it can be deduced by the lateral distribution and
thickness of sediments that meltwater continued to flow around the
detached ice blocks.
Because stratigraphic data were only collected in a north-south
direction and vertically, the lateral variation in sediments in the
east-west direction is lacking. Some information can be deduced from the
materials map (Fig. 3) and field observations. These show that following
retreat of the Hiram ice, possibly meltwater and eventually local runoff
was ponded in low areas between bedrock highs adjacent to the valley and
morainal deposits within the valley. Lacustrine deposits (Fig. 3) imply
that several large lakes formed in the valley of Mud Brook and probably
contained water until naturally drained by integration of the Mud Brook
drainage network or artificially by early settlers in the area. These
lake beds are not perfectly flat and contain low knolls of diamict
suggestive of drowned ground moraine.
This study has illustrated the late glacial stratigraphy of buried
valley sediments in the direction of ice flow. It has shown the
similarity of processes of advancing ice during late Wisconsinan
glaciations and the superposition of glacial sediments to form the
modern landscape. This study also illustrates the importance of using
combined data from a variety of sources to better understand the glacial
stratigraphy of an upland area.
ACKNOWLEDGMENTS. The authors thank the Ohio Department of
Transportation for access to borehole logs and permission to sample
roadcuts and drill additional holes along State Route 8 between Graham
Road and State Route 303. We also thank Thomas George and URS
Corporation for providing borehole logs and samples for State Route 8
between 1-271 and Twinsburg Road. The comments of five anonymous
reviewers are greatly appreciated.
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and their weathering profiles in Illinois, Part II. Weathering profiles.
Urbana (IL): Illinois State Geological Survey Circular 400.76 p.
Wilson, CGH. 1991. The origin and relative age of kames in Stow and
Hudson townships, Summit County, Ohio [Unpubl MS thesis]. Akron (OH):
Univ. of Akron. 113 p.
JOHN P. SZABO (1), CHRISTINE G. HUTH-PYSCHER and VAUGHN A. KUSHNER,
Department of Geology & Environment Science, University of Akron,
Akron, OH USA
(1) Address correspondence to John P. Szabo, Department of Geology
& Environment Science, University of Akron, Akron, OH 44325 USA,
Email: jpszabo@uakron.edu
TABLE 1
Tentative correlations of lithologic units in north-central
and northeastern Ohio
Time Killbuck Cuyahoga Grand River
Lobe Lobe Lobe
Late Ashtabula Till
Wisconsinan Hiram Till Hiran Till Hiram Till
Hayesville Till Lavery Till Lavery Till
Navarre Till Kent Till Kent Till
Middle
Wisconsinan
through
Sangamonian
Illinioan Northampton Till Northampton Till not found
Millbrook Till Mogadore Till Titusville Till
Keefus Till
Prelllinoian Mapledale Till? Mapledale Till
TABLE 2
Laboratory data for deposits in the areas of cross section A-A'
(Kushner 2006) and cross section C-C' (Wilson 1991)
Cross Section sand * silt * clay * cal dol
Unit % % % % %
A-A'
Hiram diamict
x ** 36 42 22 0.3 0.5
s 27 2 45 0.2 0.0
n 2 2 2 2 2
Hiram interbedded silt & clay
x 4 60 36 5.2 4.8
s 10 23 24 2.6 2.2
n 45 45 45 45 45
Hiram interbedded sand. silt & clay
x 14 60 26 3.7 5.1
s 22 29 29 2.3 2.6
n 12 12 12 12 12
Lavery diamict
x 12 52 36 3.6 4.3
s 10 21 22 1.7 1.3
n 15 15 15 15 15
Lavery interbedded silt & clay
x 3 56 40 3.1 4.4
s 5 24 24 1.0 1.2
n 30 30 30 30 30
Lavery interbedded sand. silt & clay
x 28 44 28 2.5 4.2
s 25 21 16 1.2 1.7
n 25 25 25 25 25
Lavery sand & gravel
x 51 40 9 3.3 4.9
s 25 25 10 1.4 1.6
n 18 18 18 18 18
C-C'
Hiram diamict
x 14 67 19 7.7 4.8
s 10 9 7 2.7 2.2
n 51 51 51 28 28
Lavery diamict
x 14 69 17 4.7 4.2
s 8 8 8 2.1 1.5
n 129 129 129 90 90
Lavery sand
x 45 46 9 3.9 7.2
s 9 6 6 1.6 0.9
n 7 7 7 6 6
Kent diamict
x 19 68 13 1.2 3.2
s 10 8 8 0.8 1.1
n 45 45 45 43 43
Kent silt
x 13 81 6 1.1 4.6
s 7 8 5 0.8 0.8
n 22 22 22 22 22
Kent sand
x 50 46 4 1.5 4.0
s 10 10 5 0.8 1.3
n 34 34 34 32 32
Cross Section tot carb DI carb clst xtln
Unit % % % %
A-A'
Hiram diamict
x ** 0.8 2.4 n.a n.a n.a
s 0.2 1.7
n 2 2
Hiram interbedded
x 10.0 1.7 n.a n.a. n.a.
s 3.9 0.6
n 45 43
Hiram interbedded sand. silt & clay
x 8.9 1.8 n.a. n.a. n.a.
s 4.8 0.7
n 12 12
Lavery diamict
x 7.9 1.5 n.a. n.a. n.a.
s 2.3 0.3
n 15 15
Lavery interbedded silt & clay
x 7.5 1.6 n.a. n.a. n.a.
s 1.8 0.3
n 30 30
Lavery interbedded sand. silt & clay
x 6.8 1.9 n.a. n.a. n.a.
s 2.7 0.7
n 25 24
Lavery sand & gravel
x 8.2 1.8 n.a n.a n.a.
s 2.6 0.4
n 18 18
C-C'
Hiram diamict
x 12.6 n.a 16 78 6
s 3.9 11 9 4
n 28 49 49 49
Lavery diamict
x 8.9 n.a. 15 78 7
s 3.0 8 8 4
n 90 129 129 129
Lavery sand
x 11.1 n.a. 14 75 11
s 1.5 7 10 3
n 6 7 7 7
Kent diamict
x 4.4 n.a. 13 79 8
s 1.5 6 6 4
n 43 45 45 45
Kent silt
x 5.7 n.a. 21 74 5
s 1.2 6 8 4
n 22 22 22 22
Kent sand
x 5.5 n.a 15 78 7
s 1.8 7 9 4
n 32 34 34 34
* Percentages of sand, silt and clay are based on matrix weights
after gravel was removed
** x = mean, s = standard deviation, n = number of samples,
cal = calcite, dol = dolomite, total carb = total carbonate,
DI = diffraction intensity ratio, carb = carbonates, clst = classics,
xtln = crystallines, n.a. = not analyzed
