Tri-State Field Conference 1980: Red Till Stratigraphy In Eastern Wisconsin

Steven Dutch, Professor Emeritus, Natural and Applied Sciences, Universityof Wisconsin Green Bay

M. C. McCartney
Residuals Management Technology
1406 East Washington Avenue
Madison, WI 53706


The purpose of this field trip is to examine some of the exposures of redtills in eastern Wisconsin and to discuss their stratigraphic relationshipsand implications to the late-glacial history of the area. The distributionof till sheets in the area is shown on Figure 1. We will examine depositsof the eastern limb of the Green Bay Lobe (at De Pere and Brillion) and ofthe western limb of the Lake Michigan Lobe (at Valders and Two Creeks).The till names used in this field trip guide are informal; the WisconsinGeological and Natural History Survey is planning to publish formal descriptions and definitions. This report is largely a summary of the informationin papers by Acomb, et al., (in preparation) and McCartney and Mickelson(in preparation).

Brief Review Of Red Till Stratigraphy (The Valderan Problem)

Recent investigations of the red tills in eastern Wisconsin have raisedquestions about the classical interpretations of the late glacial historyof the area. Studies of deposits of both the Green Bay and Lake MichiganLobes have resulted in revisions of time-stratigraphic and rock-stratigraphicnomenclatures and reinterpretations of late-glacial climatic history(Evenson, et al., 1976; Acomb, 1978; McCartney, 1979). The development ofthese changes is merely outlined here; Evenson (1973) presents a thoroughreview of the topic for the deposits of the Lake Michigan Basin.

When Chamberlin (1877) first reported on the red clay of the Lake Michiganshoreline, he correctly described the deposit at Milwaukee as stratigraphically below a similar red clay in northern Manitowoc and Kewaunee Counties.Goldthwait (1907, 1907, 1908) described the Two Creeks Forest Bed and recognized the red clay as a till. He interpreted the forest bed as documentingthe retreat and readvance of ice. Alden (1918) erroneously assigned an Illinoian age to the lower red till. Thwaites (1943) mapped a single redtill and gave it the name Valders for the red till at the Valders quarry.Thwaites and Bertrand (1957) extended the term to include the red till overthe Two Creeks Forest Bed and the red till they mapped in the Green BayLobe deposits. The term Valders or Valderan was subsequently used for redtill in the Green Bay lowland, for red till as far south as Milwaukee, Wisconsin and for tills in Michigan (e.g. Black, 1966, 1969; Bretz, 1951;Melhorn, 1954). Frye and Wilirnan (1960), Frye et al., (1968) and Wilirnanand Frye (1970) assigned the name Valderan Substage to the time span represented by the till and lacustrine deposits over the Two Creeks Forest Bed;the time span represented by the forest bed was named the Twocreekan Sub-stage.

Figure 1. Distribution of tills in the Green Bay Lobe and adjacentLake Michigan Lobe in eastern Wisconsin. Large lettersare till units, Italic letters are locations (D=De Pere,B=Brillion, V=Valders, TC=Two Creeks), arrows indicate ice-flow direction.

Recent studies on the red till stratigraphy in eastern Wisconsin (Evenson,1973; Evenson and Mickelson, 1974; Lineback, et al., 1974; Acomb, 1978;McCartney, 1979) suggest there are several post-Middle Woodfordian red tillsheets. One of these units, the Two Rivers till, is stratigraphically abovethe Two Creeks horizon and, in the Lake Michigan Basin, three till sheetsare below the forest bed (Acomb, 1978; Acomb, et al., in preparation). Twored till sheets underlie the forest bed in the Green Bay Lobe deposits(McCartney, 1979; McCartney and Mickelson, in preparation). These lowertill units are presumed to be Port Huron or Late Woodfordian age. (about13,000 years B.P.). Evenson. (1973) used geomorphic evidence, and Acomb(1978) traced the stratigraphic and areal extent of the till sheet to demonstrate that the Valders till is stratigraphically below the Two Creekshorizon. Proof of this relationship requires one section, in which theValders till definitely underlies the forest bed, but such a section hasnot been found. However, McCartney and Mickelson (in preparation) have, onthe basis of geomorphic evidence also noted by Black (1979), correlatedthe Valders till with a till in the Green Bay Lobe deposits. This GreenBay Lobe till (Chilton till) has been found under the forest bed in twoplaces.

Evenson et al., (1976) suggested replacing the time term Valderan withGreatlakean to minimize the confusion that could result from rock and timeterms with the same name that are not the. same age. Lineback et al., (1974,1979) and Black (1966, 1979) have argued against the conclusions of Evensonet al. (1976) and the change in the terminology has not yet been fullyaccepted. However, the investigations of Acomb (1978), McCartney (1979),McCartney and Mickelson (in preparation) and Acomb et al., (in preparation)support the basic conclusions of Evenson (1973) and further indicate thatthe time term Valderan should be. replaced.

A major result of the work by Evenson et al., (1976) is that "the Two Creeksand Valders are no longer viewed, as outstanding events of Lake MichiganLobe history. Instead of one major readvance of the ice, the red tillsrepresent minor readvances of a generally receding ice front. Further,the Gary-Port Huron Interstade preceding the advance of the ice. whichdeposited the red tills is now recognized as an event of major significancein the Lake Michigan Lobe. Thus, the history of the Lake. Michigan Lobesince the Middle Woodfordian includes a major deglaciation (Gary-Port HuronInterstade) followed by readvances (Port Huron) of somewhat less magnitudethan the Gary about 13,000 years B.P. with a minor deglaciation (Twocreekan)and a final period of minor readvance (Greatlakean) about 11,800 years, B.P.According to Saarnisto (1974), the Lake Michigan Basin became ice-free around11,000 years B.P.

The interpretation of the Lake Michigan Lobe late-glacial history is nowconsistent with what is known about the area to the east. That is, theGary-Port Huron Interstade is now considered an important event in the LakeMichigan Lobe. This retreat has long been recognized in the eastern GreatLakes (Evenson and Drelmanis, 1976). In Michigan it is represented by theCheboygan byrophyte bed which is buried by red till of Port Huron age(Farrand et al, 1969). Further, the Twocreekan Substage is now consideredto be a minor event. This is consistent with the pollen evidence whichindicates progressive deglacliation without major reversals in the northwardadvance of plant communities (Evenson et al, 1976).

Rock-Stratigraphic Units


The tills of the Green Bay Lobe correlate with those of the Lake Michigan Lobe; however, because the two lobes traversed different bedrocks, correlated till sheets differ llthologically. On that basis, separate rock-stratigraphic nomenclature is required for the two lobes. For the same reasons, separate nomenclature is also required for the western and eastern limbs of the Green Bay Lobe.

Table I summarizes the till stratigraphy and correlations of the Green Bayand Lake Michigan Lobes. Advances of the Green Bay Lobe deposited at leastthree red till sheets which are Late Woodfordian age and younger. In thewestern part of the lowland, the tills are distinguished on the basis ofstratigraphic position, texture, color and depth of leaching. In the central part of the lowland, tills are covered by lacustrine sediment, but onthe east side a similar sequence of tills is present. Here till units aredistinguished on the basis of texture and magnetic susceptibility. In theLake Michigan Lobe, four Late Woodfordian age and younger tills are distinguished by differences in stratigraphic position, grain-size distribution,and clay mineral content. The Chilton till of the Green Bay Lobe, which isoverlain by Twocreekan wood at two localities, correlates with the Valderstill of the Lake Michigan Lobe. In both lobes, a Greatlakean till overliesthe forest bed at several localities.

Table I: Correlation Of Till And Forest Bed Units Of The Green Bay And Lake Michigan Lobes

  Time Stratigraphy Stages of Glacial Lake Chicago Western Green Bay Lobe (McCartney, 1979) Eastern Green Bay Lobe (McCartney and Mickelson, in prep.) Western Lake Michigan Lobe (Acomb et al., in prep.) Lake Michigan (Lineback et al., 1974) Eastern Lake Michigan Lobe (Farrand et al., 1969; Evenson, 1973, Taylor, 1978)
  Greatlakean ?? Middle Inlet Glenmore Two Rivers Two Rivers Two Rivers
Ca. 11,800 Twocreekan Calumet Two Creeks Forest Bed Two Creeks Forest Bed Two Creeks Forest Bed    
  Late Woodfordian

(Port Huron)

Glenwood Kirby Lake Chilton Valders Manitowoc Inner Port Huron (Manitowoc)
  Silver Cliff Branch River Ozaukee Shorewood Outer Port Huron (Shorewood)
Ca. 13,000           Cheboygan bryophyte bed

Green Bay Lobe Deposits

In the western limb of the Green Bay Lobe, the red till units overlying thebrown, sandy, Middle Woodfordian Mapleview till are, in ascending order, theSilver Cliff, the Kirby Lake, and the. Middle Inlet tills (Figure 1). In theeastern limb of the lobe, the corresponding units overlying the brown, sandy,Middle Woodfordian Wayside till are the Branch River, the Chilton, and theGlenmore tills. The tills on either side of the lobe are physically separatedby sediment of Glacial Lake Oshkosh (Figure 1). The Silver Cliff till is adull, reddish-brown, sandy loam, which is slightly siltier (Figure 2) thanthe underlying Mapleview till. The Silver Cliff, and the Kirby Lake tillwhich overlies it, are Late Woodfordian (Port Huron) age. The Kirby Laketill is finer grained (less than 50% sand) and usually redder than theother units. This till has more variability than tills above and below,and it is possible that it represents two ice advances, which deposited tillof similar composition. The Kirby Lake till is overlain by the Middle Inlettill, which is dull reddish brown to dull brown, sandy loam. This till isvery similar to the Silver Cliff and is best distinguished from it by its stratigraphic position. Where Silver Cliff till or Middle Inlet till arepresent at the surface, they can be distinguished by depth of carbonateleaching. Carbonates are leached deeper than 1 m in the Silver Cliff till and less than 30 cm in the Middle Inlet till. A number of sites (McCartney,1979) show two or three till units in one section, and the stratigraphicposition of the units is well established.

Figure 2. Triangular diagram showing sand/silt/clay percentagesof the 4 tills on the western side of the Green Baylowland. Shaded areas show distribution of 54 samplesof Middle Inlet till, 33 samples of Kirby Lake till,33 samples of Silver Cliff till and 32 samples ofMapleview till.

Figure 3. Plot of sand (2 - 0.0625mm) fraction vs. magnetic susceptibilityof the less than 2mm fraction of tills on the east side of theGreen Bay lowland. Magnetic susceptibility measured on 30gmsamples.

Other lithologic properties of the tills are shown in Table II. Additional lithologic information and trend-surface analyses of lithologic parametersare given in McCartney (1979).

The western limit of the Silver Cliff till is the red-till boundary of GreenBay Lobe deposits as mapped by Leverett (1929), and its age apparentlycorrelates with one of the outer red till units in the Lake Michigan lowland which are Late Woodfordian (Port Huron) age. The Kirby Lake is alsoLate Woodfordian age, and its western boundary is the edge of the Valdersof Thwaites (1943). The western limit of the Middle Inlet till, which wasdeposited during Greatlakean time, coincides with the Athelstane moraine(Thwaites, 1943).

On the east side of the Green Bay lowland a similar sequence of tills ispresent, but here grain size and magnetic susceptibility are used tocharacterize the tills (Figure 3). The sandy Branch River till with highmagnetic susceptibility is the oldest Port Huron till and can be seenoverlying the Middle Woodfordian Wayside till at several localities. Abovethis is the finer grained (Figure 3) Chilton till, which directly underliesthe forest bed at two localities (Figure 4). Like its counterpart at thewest side. of the lowland, this unit may represent more than one ice advance.Its texture is more variable than either of the other red tills (Figure 3).Depth of the carbonate leaching on the Branch River and Chilton tills isdeeper than 70 cm.

The Greatlakean Age Glenmore till is leached a maximum of 75 cm althoughdepth of leaching is generally considerably less. In addition, the Glen-more till has consistently lower magnetic susceptibility than the pre- Twocreekan units (Figure. 3). Other characteristics of these tills aregiven in Table II.

Lake Michigan Lobe Deposits

The four red till units in the Lake Michigan Lobe are in ascending order,the Ozaukee, the Haven, the Valders, and the Two Rivers. The Ozaukee tillis distinguished from the other red tills by its fine grain-size distribution (Figure 5, Table II). This till is also distinguished by its consolidation. The Ozaukee till is normally consolidated to slightly overconsolidated, but the younger red tills are significantly overconsolidated.This may be due to the presence of permafrost during deposition of theOzaukee till (Mlckelson et_al., 1979). The Haven till, which overlies the Ozaukee, is siltier than the Ozaukee till and has a clay mineralogy nearlyidentical to it (Figure 5, Table II). The Haven is the red-to-gray tillexposed below the Two Creeks Forest Bed, and in almost every shorelineexposure it is overlain and underlain by lake sediments up to the Glenwoodlevel (640'). The Valders till can be distinguished from the underlyingHaven and Ozaukee tills by its clay mineralogy and grain size (Figure 5, Table II); clay mineralogy differentiates the Valders from the Two Rivers till. The Two Rivers till can be differentiated from the Haven and Ozaukeetills by grain-size distribution. Depth of carbonate leaching in the TwoRivers till is much shallower than in the older red tills (Mickelson and Evenson, 1975). The stratigraphic relationship of these red tills is shownin Figure 6.

Table II

haracteristics Of Lake Michigan Lobe Red Tills. First Parenthesis is Standard Deviation, Second Parenthesis is Number Of Samples

  % Sand % Silt % Clay % Illite Expandable % Chlorite-Kaolinite Calcite-Dolomite Ratio % Total Carbonate Magnetic Susceptibility Predominant Color
Two Rivers 31(3.9)(11) 50{6.1)(11) 19(5.3)(11) 52(3.5)(42) 35(4.0)(42)  13(2.6)(42) .17(.2)(10) 39.2(8.4)(10) 4.3(.8)(18) 5YR6/3
Valders 30(8.6)(33) 52(8.1)(33) 18(7.9)(33) 42(3.7)(53) 46(5.0)(53) 12(2.7)(53) .12(.1)(10)   40.2(2.7)(10) 5.4(1.6)(22)  5YR6/4
Haven 16{7.1)(27) 56(6.2)(27) 28(6.6)(27) 56(5.0)(58) 25(4.5)(58) 19(3.2)(58) .10(.l)(10) 36.4(9.6)(10) 5.0(1.0)(22) 5YR6/4
Ozaukee 13(3.9)(19} 47(5.0)(19)  40(6.5)(19) 60(5.1)(20) 20(5.8)(20)         5Y6/4
  1. Percent of <2 mm fraction. Boundaries used are 2mm, 00625 mm. and 0,002 mm.
  2. Relative clay mineral percentages of <2 mm fraction. Method modified from Glass (personal communication, 1977).Method outlined in Acomb, 1978.
  3. Based on Chittick analysis of <.0625 mm fraction.
  4. Based on measurement of 30 mm. subsample of <2 mm fraction.

Figure 6. Correlation of tills in the Two Rivers, Two Creeks, Valders area. Tills (large letters); TR, Two Rivers;V, Valders; H, Haven; 0, Ozaukee; U, Unnamed (Gary).Other (small letters); g, gravel; 8, sand; sl, slit;c, clay; dol, dolomite. Location of section shown bysymbol on Figure 1.

Three of the four red tills in the Lake Michigan Lobe are believed to beLate Woodfordian or Port Huron in age: the Ozaukee, the Haven, and the Valders. The Two Rivers till is post-Twocreekan or Greatlakean in age.The Valders till is interpreted to be pre-Twocreekan because it is correlative with the Chilton till which has been found below the forest bed. Theage-equivalency of these two tills is based on geomorphic evidence. TheValders till has a clear ice margin with unpitted outwash where it overrides the Branch River and Wayside tills (Figure 1); however, where the Valders abuts the Chilton till there is no distinct ice margin and no unpitted outwash. This evidence suggests there was ice in both lobes atthe time the Valders and Chilton tills were deposited (Black, 1979; McCartneyand Mickelson, in preparation).


The age of the Valders till is the major source of disagreement in interpretations of the late-glacial history of eastern Wisconsin. The change interminology from Valderan to Greatlakean for post-Twocreekan time isrequired because of the "non-Valderan" age of the Valders till. Someworkers (Lineback t a., 1974, 1979; Black, 1966, 1969, 1979) are notconvinced that the Valders till is pre-Twocreekan and have not adopted the. new terminology. Recent investigations (Acomb, 1978; McCartney, 1979;McCartney and Mickelson, in preparation; Acomb, et al. in preparation)support Evenson's (1973) conclusion that the Valders till is pre-Twocreekan.

As previously mentioned, proof that the Valders till is pre-Twocreekanrequires an exposure with both the Valders till and the forest bed. Althoughno such section has been found, the weight of evidence suggests a pre-Twocreekan age for the Valders till. In particular, the presence of pre-Twocreekan Glenwood shorelines (Eschman and Farrand, 1970) cut into the Valders till surface north, of Manitowoc (Evenson, 1973) and the correlationof the Valders with the clearly pre-Twocreekan Chilton till (McCartney andMickelson, in preparation) are the most cogent of several arguments (Acomb,et_ al.. in preparation) In favor of the pre-Twocreekan age of the Valders till. Other evidence includes significantly greater depth of carbonateleaching on the Valders and Chilton till surfaces than on the Two Riversand Glenmore tills (Mickelson and Evenson, 1975; McCartney and Mickelson,in preparation) and the occurrence of forest beds buried by till onlywithin the limit of the Two Rivers-Glenmore-Middle Inlet boundaries.Finally, although the Valders till has not been found below the forest bed,' neither has it been found above it. The Chilton till, however, has beenfound below the forest bed, and this till is interpreted to be the time-equivalent of the Valders (Black, 1979; McCartney and Mickelson, in preparation) .


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