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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

mailto: [email protected]

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


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


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



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).



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



(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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