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This chapter was originally published in the book Developments in Quaternary Science, Vol.15, published by Elsevier, and the attached copy is provided by Elsevier for the author's benefit and for the benefit of the author's institution, for non-commercial research and educational use including without limitation use in instruction at your institution, sending it to specific colleagues who know you, and providing a copy to your institution’s administrator.
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From: John P. Szabo, Michael P. Angle and Alex M. Eddy, Pleistocene Glaciation of Ohio, USA. In J. Ehlers, P.L. Gibbard and P.D. Hughes, editors: Developments in
Quaternary Science, Vol. 15, Amsterdam, The Netherlands, 2011, pp. 513-519. ISBN: 978-0-444-53447-7.
© Copyright 2011 Elsevier B.V. Elsevier.
Author's personal copy
FIGURE 39.1 Topographically contr
the southern terminus of the Laurentide
the boundary between the Central Lowl
Plateaux to the east.
Developments in Quaternary Science. Vol. 15, doi: 10.1016/B978-0-444-53447-7.00039-8
ISSN: 1571-0866, # 2011 Elsevier B.V. All rights reserved.
Chapter 39
Pleistocene Glaciation of Ohio, USA
John P. Szabo1,*, Michael P. Angle2 and Alex M. Eddy2
1Department of Geology & Environmental Science, University of Akron, Akron, Ohio 44325-4101, USA2Ohio Department of Natural Resources, Division of Geological Survey, 2045 Morse Road, Building C-1, Columbus, Ohio 43229-6693, USA
*Correspondence and requests for materials should be addressed to John P. Szabo. E-mail: [email protected]
39.1. INTRODUCTION
The article of Szabo andChanda (2004) is herein expanded to
providemuchmoredetail into theglaciationofOhio.Littlehas
changed in our knowledge of Early Pleistocene glaciations,
but a summary of extensive research into the stratigraphy of
the Illinoian Stage of the Middle Pleistocene (Szabo and
Totten, 1995) is included. Additionally, recent work of
ThomasLowell at theUniversity ofCincinnati on datingLate
Pleistocene advances in western Ohio is discussed. A brief
summary of the history of late-glacial and post-glacial Lake
Erie and its effect on drainage systems is also presented. A
mapof the distributionof beach ridges is included inArcView
in addition to maps of the limits of glaciation and moraines.
Information on the general geology of Ohio is useful in
understanding its glaciation. The Portage Escarpment
(Fig. 39.1) is the boundary of two major physiographic
provinces that occur in Ohio. Eastern Ohio lies within the
Allegheny Plateaux (Brockman, 1998), which is capped
in most places by resistant Pennsylvanian-aged sandstones.
Western Ohio is lower in elevation and is part of the Central
Lowlands; bedrock consists predominately of carbonate
rocks. As ice flowed into the Erie Basin from the north or
at times from the northeast, its spread southward was
controlled by these physiographic provinces. Ice split into
topographically controlled sublobes; herein referred to as
lobes (Fig. 39.1). The Miami and Scioto lobes flowed much
farther south through the Central Lowlands, whereas the
Killbuck, Cuyahoga and Grand River lobes flowed onto
the higher elevations of the plateaux.
olled sublobes of the Erie Lobe at
ice sheet in Ohio. Dashed line is
ands to the west and the Allegheny
39.2. TERTIARY PERIOD
There is no evidence of Tertiary glaciations in Ohio, but
there are sands of questionable origin on high divides south
of the glacial boundary near Dresden (D, Fig. 39.2). Nine
metres of loess and possible aeolian sand overlie at least
6 m of Mn-stained fluvial sands. The intensity and
thickness of this staining have not been found in fluvial
deposits north of the glacial boundary and may be sugges-
tive of weathering over a long period of time. Other ‘black’
sands have been reported in water wells south of the glacial
boundary. There is insufficient evidence to determine if
these sands originated during the Tertiary or are the product
of some Early Pleistocene glaciation.
39.3. EARLY PLEISTOCENE GLACIATIONS
Magnetically reversed lacustrine sediments, Minford Silt,
in abandoned valleys of the Teays drainage system provide
evidence of an Early Pleistocene glaciation in at least the
513
FIGURE 39.2 Glacial limits, end moraines and key locations in Ohio. A, Akron; C, Cincinnati; CG, Cuba Gully; CL, Cleveland; CV, Cuyahoga Valley;
D, Dresden; DM, Defiance Moraine; FW–WM, Fort Wayne–Wabash Moraine; G, Gahanna; GC, Granny Creek; GH, Garfield Heights; L, Lancaster;
LCI, London Correctional Institute; MG, Mt. Gilead; NL, North Lima; OX, Oxford; PGL, Pingrove Landfill; SC, Swine Creek; SWL, Southwest
Licking; TF, Todd Fork; UC-PM, Union City-Powell Moraine.
Quaternary Glaciations - Extent and Chronology514
Author's personal copy
northern half of Ohio. The Minford Silts are older than
780,000 years (Szabo and Chanda, 2004). A possibly older
deposit, Calcutta Silt (Lessig, 1963; Fullerton, 1986), is
found at high elevations near the Ohio–Pennsylvania
state line.
Attempts have been made to integrate many buried val-
leys in Ohio into the Teays drainage (Stout et al., 1943).
However, a complex network of buried valleys incised into
bedrock underlies most of glaciated Ohio; efforts to connect
all buried bedrock valleys into one drainage network lead to
impossibly complex unnatural patterns (Frolking and
Szabo, 1998). Many deep valleys (>70 m) are orientated
approximately north–south and are generally filled with
lacustrine deposits indicative of ice damming (Szabo,
2006). The lower parts of their cross-sections are generally
V-shaped, whereas their upper parts have been glacially
modified (Szabo, 1987). These are possible remnants of
drainage during Tertiary or Early Pleistocene time. Gener-
ally, shallower buried valleys (<70 m) may have formed
along ice-front positions or by meltwater draining south-
ward from the ice sheet towards the ancestral Ohio
River throughout the latter part of the Pleistocene Epoch
(Szabo, 2006).
39.4. MIDDLE PLEISTOCENEGLACIATIONS
Little work has been done in the pre-Illinoian area beyond
the Illinoian limit (Fig. 39.2), nor has much been done
within the area mapped as Illinoian surficial materials.
Within these two areas, possible Middle Pleistocene sedi-
ments could be exposed in deeply incised stream valleys
or in deeper borings for water wells. The Illinoian end
moraine as mapped on the glacial map of Ohio (Pavey
et al., 1999) may not represent the actual maximum extent
of Illinoian ice; erratic boulders often are found beyond the
mapped limit suggesting erosion of either older glacial
deposits or thin Illinoian sediments (White, 1982). The
Illinoian moraine is generally more subdued than its
Chapter 39 Pleistocene Glaciation of Ohio, USA 515
Author's personal copy
Wisconsinan equivalent, consisting of broad, gently rolling
hills. Illinoian ground moraine is found between the Illi-
noian and Wisconsinan terminal moraines and is generally
dissected having a well-integrated drainage compared to
that of Wisconsinan ground moraine.
Sites exposing sediments from the early part of the Mid-
dle Pleistocene are not easily identified (Szabo and Chanda,
2004). In a 100-m deep borehole into a buried bedrock val-
ley in southwestern Licking County (SWL; Fig. 39.2), at
least 50 m of Illinoian glacial sediments overlie older tills
and laminated fines that appear to have normal magnetic
polarity (Frolking and Szabo, 1998). In north-central and
northeastern Ohio, multiple Illinoian-age units have been
differentiated (Szabo and Totten, 1995), whereas in south-
western Ohio, only one unit, Rainsboro Till, has been iden-
tified (Rosengreen, 1974; Quinn and Goldthwait, 1985).
At Mount Gilead (MG) in central Ohio (Fig. 39.2), several
tills underlie silt (loess?) having a themoluminescence (TL)
date from near the end of theMiddle Pleistocene (Szabo and
Chanda, 2004). Tills beneath this loess were separated
based on percentages of calcite and dolomite in their
<0.074-mm fractions and were traced northward and east-
ward to establish the stratigraphy illustrated in Table 39.1.
The two lowermost tills at this section are currently insep-
arable and are referred to as the Chesterville Till best
exposed at Granny Creek (GC; Fig. 39.2). This unit contains
nearly 2% calcite and 9% dolomite (Szabo, 2006) and is
overlain by the Gahanna Till (G; Fig. 39.2) having up to
20% fine carbonate.
The most areally extensive unit found at MG is the
Millbrook Till and its equivalents (Table 39.1) containing
almost no calcite and 4–6% dolomite depending on loca-
tion. Its total fine-carbonate content declines eastward in
Ohio and allows this unit to be used as a marker bed from
TABLE 39.1 Tentative Correlations of Lithologic Units in Nor
Time
Scioto lobe
Northern Eastern
Late Wisconsinan(Weichselian)
Hiram Till Hiram Till
Hayesville Till Hayesville Till
Navarre Till Navarre Till
Middle Wisconsinan(Weichselian) throughSangamonian (Eemian)
Millbrook Till U Millbrook Till U
Millbrook Till M Northampton Till
Illinioan (Saalian) Millbrook Till L Millbrook Till
Gahanna Till
Chesterville Till
central Ohio into adjacent western Pennsylvania (Szabo and
Totten, 1995). A representative section of equivalent Titus-
ville Till (Table 39.1) is exposed in the valley of Swine
Creek (SC) in northeastern Ohio (Fig. 39.2). Analysis of
tills at this section (Szabo, 2006) identified a repetition of
textural and compositional properties reflective of thrust
stacking as proposed by Moran (1971). Heavy-mineral
studies of the tills in this section show that their provenance
is in the Madoc–Arnprior area of the Grenville province in
Canada (Matz, 1996; Szabo, 2006), whereas analysis of
equivalent Millbrook Till at MG shows a source area on
the north shore of Lake Huron in the Superior-Southern
province (Matz, 1996). Other evidence for thrust stacking
is present in strip mines in eastern Ohio; Franko (2008) de-
lineated compositional differences between meltout tills
and deformational comminution tills at North Lima (NL;
Fig. 39.2).
Other Illinoian units overlie the Millbrook Till and its
equivalents (Table 39.1). The moderately calcareous, more
clay-rich Northampton Till overlies the Millbrook Till and
its equivalent Mogadore Till in north-central and western
northeastern Ohio (Szabo and Totten, 1995). This unit is
very firm and has intensely oxidised joints exposed where
it outcrops in deeply incised tributaries in the valley of the
Cuyahoga River (CV; Fig. 39.2). A sandier, less consoli-
dated till, informally referred to asMillbrook Till U is found
north of MG (Fig. 39.2) along the eastern edge of the area
glaciated by the Scioto lobe and extends into the northern
portion of this lobe.
Several problems exist in defining and correlating units
of the Middle Pleistocene, more specifically those of the
Illinoian Stage. Dating of advances of this stage is not well
constrained, relying on established observational criteria
summarised in (White, 1982); however, no other dates
th-Central and Northeastern Ohio
Killbuck lobe Cuyahoga lobe Grand River lobe
Ashtabula Till
Hiram Till Hiram Till Hiram Till
Hayesville Till Lavery Till Lavery Till
Navarre Till Kent Till Kent Till
Northampton Till Northampton Till Not found
Millbrook Till Mogadore Till Titusville Till
Keefus Till
Quaternary Glaciations - Extent and Chronology516
Author's personal copy
are available, and a Late Wisconsinan till overlies the TL-
dated silt at MG. Another common marker horizon used to
differentiate Illinoian from Wisconsinan deposits is the
presence of a Sangamonian soil that is missing throughout
much of northern Ohio (Szabo, 1997). This soil was formed
in Illinoian tills of southwestern Ohio (Hall and Zbiesz-
kowski, 2000) and in Illinoian loess in southeastern Ohio
(Frolking and Szabo, 1998), but it is not found in sections
in the northern part of the state. Sharp contacts between
unweathered Illinoian tills and their overlying Wisconsinan
tills suggest erosion before or during the Late Wisconsinan
advances. Not much mapping on a countywide basis has
occurred since the end of the state-sponsored programme
in the late 1980s. Thus, workers have been unable to corre-
late isolated outcrops in the area glaciated by theMiami and
western Scioto lobes in western Ohio with the better-estab-
lished Illinoian stratigraphy from the eastern Scioto lobe
and other lobes in northern Ohio.
39.5. LATE PLEISTOCENE GLACIATIONS
The normal geological processes including pedogenesis
that operate on landscapes began during the Sangamonian
Stage interglacial and continued through climate oscilla-
tions of Early and Middle Wisconsinan time. Calculation
of ice volumes based on sea-level curves suggests that there
was not enough ice during these parts of the Wisconsinan
Stage to glaciate Ohio (Clark and Lea, 1992). Specimens
of wood collected from gravels deposited during this time
all have ‘greater than’ dates and contain both deciduous
hardwoods from warm periods and spruce from cold
periods (Goldthwait, 1958). A few dates in the 40 14C ka
range suggest a warm period during which colluviation of
FIGURE 39.3 Section at Garfield Heights, Ohio (modified from White, 19
slopes and alluvial fan deposition occurred (Goldthwait,
1992; Hall and Zbieszkowski, 2000).
Additional evidence suggests that baselevels of streams
were lower than present, and streams were well incised into
Illinoian deposits. Parts of the Teays system may have been
exhumed because wood dated at 28.39�0.33 14C ka BP
(ISGS-3224) was found in alluvium (Lloyd, 1998; Frolking
andSzabo,1998)about75 mbelowthesurfaceinaburiedbed-
rockvalleyassociatedwith theTeays system(LondonCorrec-
tionalInstitute(LCI);Fig.39.2).AboringnearLancaster(L) in
Fairfield County (Fig. 39.2) contained at least 56 m of Late
Wisconsinan sediments, and at Pingrove Landfill (PGL) in
the same county (Fig. 39.2) wood dated at 26.78�0.43 14C
ka BP (ISGS-3223) was found in the basal Wisconsinan till
35 m below the surface in a buried bedrock valley.
The section at Garfield Heights (GH; Figs. 39.2 and
39.3) is the only location on the Allegheny Plateau in north-
ern Ohio having a nearly complete record of the Late Pleis-
tocene and has been studied periodically for over 50 years
(Szabo, 1992). The site is currently covered by vegetated
colluvium, but can be excavated to expose most of the
younger units described in the literature (Szabo, 1997).
Units older than the Illinoian Stage at this site and at an ad-
jacent site are no longer accessible; their age assignments
are discussed in Fullerton (1986) and Szabo (1992).
Gravels are the oldest accessible unit at the site (Fig. 39.3)
and are interpreted to be Illinoian age (White, 1968; Szabo,
1992). A dark reddish-brown, truncated paleosol is found in
the upper part of the gravels, and its formation has been
assigned to the Sangamonian interglacial (White, 1968).
The matrix of the gravel below the paleosol becomes calcar-
eous 25 cm below the paleosol (Miller and Szabo, 1987);
lower in the section carbonate cements layers of gravel.
68).
Chapter 39 Pleistocene Glaciation of Ohio, USA 517
Author's personal copy
Although loess overlies the paleosol near the south end of the
section (Fig. 39.3), a yellowish-brown to greenish-grey, platy
to blocky to massive accretion gley of variable texture over-
lies the gravels through most of the section to the north. Clay
mineralogy varies between layers of gley having definable
X-ray diffraction peaks associated with vermiculite and
montmorillonite and those layers having broad peaks associ-
ated with heterogeneous swelling material (Miller and
Szabo, 1987), suggestive of episodic erosion upslope.
A bipartite loess sequence (Fig. 39.3) overlies the gley
and thickens northward. The older, yellowish-brown, friable
loess is non-calcareous, and its claymineralogy also suggests
that this loess has been weathered. A weakly developed soil,
10 cm below the contact with the upper loess unit contains
disseminated organic material dated at 27.39�0.35 14C ka
BP (ISGS-1949). A wood fragment from this loess dated
at 28.195�0.535 14C ka BP (K-361-3). At some locations,
this loess has involutions accentuated by iron; Fullerton
(1986) suggested that this cryoturbated loess implies the
presence of ice in the nearby Erie Basin. The upper part of
the loess sequence consists of a light olive-brown to light
greyish-brown, calcareous, friable silt containing snails and
wood fragments (Miller and Szabo, 1987).
Laminated lacustrine silts and clays overlie the loess
sequence. The lower part of these brownish-grey, platy, cal-
careous deposits consists of sandy zone containing snails
and wood fragments interpreted as a colluvium (Miller
and Szabo, 1987). Several radiocarbon dates on wood in
this zone average about 24 14C ka BP. The fossils in the
lacustrine sequence suggest deterioration of local climate
as the ice advanced (Szabo, 1997). Dark brown, leached,
calcareous till caps the section and may represent deposi-
tion by LateWisconsinan Lavery or Hiram ice (Table 39.1).
However, about 50 m to the south, sandy Kent till of the
first LateWisconsinan advance lies between the dark brown
till and the lacustrine sediments.
The Wisconsinan limit in southwestern Ohio is defined
by well-formed moraines especially in the area covered by
the Scioto lobe (Fig. 39.2). The limit in theMiami lobe is less
well constrained bymoraines but was reconstructed based on
boulder density counts (Goldthwait et al., 1961). The termi-
nal moraine near Cincinnati (C; Fig. 39.2) has been breached
by meltwater streams and dissected by tributaries of the Mi-
ami and Ohio rivers. Figure 39.2 shows that the Allegheny
Plateaux deflected the Scioto lobe to the southwest. In areas
of both the Scioto and Miami lobes, the topography consists
of a succession of recessional moraines (Fig. 39.2) separated
by intervening areas of loamy ground moraine. Outwash
trains, kames and very short eskers are found in the interlo-
bate area between these lobes. Inter-moraine lake beds are
more common and kames less common in the poorly drained,
clay-rich tills in the northern areas glaciated by these lobes.
The Late Wisconsinan glacial limit in the Miami and
Scioto lobes is well constrained by radiocarbon dates
(Lowell et al., 1999). Several dates on organic material
and trees 2 km behind the maximum limit of ice near Todd
Fork (TF; Fig. 39.2) average about 23.2�0.086 14C ka BP.
Dates of another expansion of ice that overran trees at Cuba
Gully (CG; Fig. 39.2) average 20.36�0.084 14C ka BP
(Lowell et al., 1999). Farther west in the Miami lobe at Ox-
ford (OX, Fig. 39.2), ice overrode trees having an average
date of 20.77 14C ka BP and reached its maximum limit
north of Cincinnati (C, Fig. 39.2) at an average date of
19.59�0.035 14C ka BP (Lowell et al., 1999).
The Late Wisconsinan limit in the Killbuck, Cuyahoga
and Grand River lobes is less well defined in north-central
and northeastern Ohio (Figs. 39.1 and 39.2). Dissected
resistant bedrock affected the initial Late Wisconsinan ad-
vance onto the plateaux. Loamy tills along the glacial limit
occur as discontinuous, hummocky moraine without linear
trends in many areas (White, 1982), and the limit is often
defined by weathering criteria. Widely spaced recessional
moraines of the Scioto lobe are compressed and even merge
in the area of the Killbuck lobe; the Defiance Moraine (DM;
Fig. 39.2) is the only well-defined recessional moraine.
Very extensive outwash trains and kame deposits occupy
the re-entrant (Fig. 39.1) among the Killbuck, Cuyahoga
and Grand River lobes in northeastern Ohio. Stagnation to-
pography is common along the margins of these lobes, sug-
gesting that ice remained stationary in these areas for long
periods of time (Szabo, 2006).
Dating of the Late Wisconsinan advance in northeastern
Ohio is not well constrained because very little organic mat-
ter has been found in moraines at the limit. Based on dates
from wood at the base of the lacustrine part of the section at
GH, ice advanced onto the plateaux after 24,000 14C years
ago and had retreated to north-east of Cleveland (CL) by
14,450 14C years ago (Szabo et al., 2003). By about
16,000 14C years ago, ice had retreated into the northwards
and eastwards during the Erie Interstadial (Dreimanis and
Goldthwait, 1973) and then readvanced southwestward
from the Niagara Falls area of Ontario (Fullerton, 1986).
Ice overrode interstadial lacustrine clays and deposited
clay-rich tills over the northern half of Ohio. Probability
curves of radiocarbon dates from basal organic matter in
30 basins in Ohio and eastern Indiana show that the majority
of basins formed at either 15,500 or 14,800 14C years ago
(Glover et al., 2004). These are dates traditionally assigned
to the post-interstadial advances that formed the Union
City-Powell Moraine and the FortWayne–WabashMoraine
(UC-PM and FW–WM; Fig. 39.2), respectively (Dreimanis
and Goldthwait, 1973).
As ice retreated from northeastern Ohio at about 14.514C ka BP (Szabo et al., 2003), a series of lakes formed that
were trapped between the ice and higher topography to the
south. A series of beach ridges along the south shore of
Lake Erie remain as evidence of changing ancestral lake
levels as various outlets were exposed by deglaciation
Quaternary Glaciations - Extent and Chronology518
Author's personal copy
(Szabo et al., 2003). As ice retreated from the Niagara pen-
insula about 12.5 14C ka BP (Lewis, 1969), the last ancestral
lake in the Erie basin drained. The level of the resultant Early
Lake Erie was about 40 m below the present level (Szabo
et al., 2003) and causing extensive downcutting in drainage
systems that emptied into this lake and shifting the continen-
tal divide at Akron (A; Fig. 39.2) southwards. A post-glacial
channel is deeply incised into a till in the buried bedrock
valley of the lower CV 37 m below the present level of Lake
Erie at CL (Fig. 39.2) and possibly was formed by the rapid
drop in base level (Szabo et al., 2003). Post-glacial isostatic
rebound of the Niagara Falls area raised the outlet of Early
Lake Erie, and it filled the basin to modern levels. By about
7.18�0.070 14C ka BP (ISGS-4439), the level of the flood-
plain of the CV north of Akron was within 3 m of its present
elevation (Szabo et al., 2003).
Several problems are apparent in our understanding of
the Late Pleistocene glaciation of Ohio. The timing of the
advance of ice to its limit in northeastern Ohio is not well
constrained. Was the climate substantially different on
the Allegheny Plateau compared to the lowlands of south-
western Ohio? The recessional moraine succession in west-
ern Ohio appears to have been driven by relative ablation
rates (Lowell et al., 1999), whereas the sequence of glacial
retreat on the Allegheny Plateau in northeastern Ohio
represents an extended period of stagnation.
39.6. CONCLUSIONS
Consideration of our knowledge of the glaciation of Ohio
produces the logical conclusion that the sequence of events
creating the Late Pleistocene landscape of Ohio is better
understood than the results of earlier glaciations. The
identification of Early Pleistocene deposits relies on the
acquisition of orientated core samples from deep borings
and the use of paleomagnetic analysis. Some outcrop anal-
ysis of lacustrine sediments may be of value in the deeply
dissected, non-glaciated area of south-eastern Ohio. The
stratigraphy of the Middle Pleistocene, especially the last
glaciation, the Illinoian, is better understood in north-cen-
tral and northeastern Ohio then in western Ohio. The timing
of Late Wisconsin advances of ice during the Late Pleisto-
cene is better constrained in western Ohio than in eastern
Ohio suggesting some fundamental difference not only in
topography but also in climate.
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