INTRODUCTION
The lake cliffs along the northern shore of Lakes Erie and Ontario are among the best-studied Quaternary sections in the Great Lakes area (for history, see Karrow, Reference Karrow1967, Reference Karrow1984; Eyles and Eyles, Reference Eyles and Eyles1983; Barnett, Reference Barnett1998; Martini and Bowlby, Reference Martini and Bowlby2011). They form the basis for the eastern Great Lakes Wisconsin stratigraphy (Karrow et al., Reference Karrow, Dreimanis and Barnett2000). The main sections are north-shore cliffs at Scarborough and Bowmanville in Lake Ontario and from Port Stanley to Port Dover in Lake Erie (Fig. 1A), but these are inadequately dated and some stratigraphic relationships can be interpreted in different ways.
Ice extent in the eastern Great Lakes for: (A) Port Bruce advance, 18 ka; (B) Port Huron advance, 15 ka (after Larson and Schaetzl, Reference Larson and Schaetzl2001); (C) glacial retreat moraines in Lake Erie basin (modified from Barnett and Karrow, Reference Barnett and Karrow2018).
The retreat of the Erie Lobe from its last glacial maximum (Nissouri phase) in southern Ohio began around 27 ka, as shown by dates of 27.16 ± 0.32 and 27.3 ± 0.5 ka from wood in lake silts behind the Cuba moraine (Lowell et al., Reference Lowell, Hayward and Denton1999; Dyke et al., Reference Dyke, Andrews, Clark, England, Miller, Shaw and Veillette2015; Nash, Reference Nash2020). It took about 12 ka to retreat to near the eastern end of Lake Erie, as shown by the dates of 14.8 ± 0.2 and 14.9 ± 0.22 ka from the Winter Gulf peat in lake deposits above the Lake Escarpment moraine (Thatcher Till) at Gowanda, south of Buffalo (Calkin, Reference Calkin, Buehler and Calkin1982; Szabo et al., Reference Szabo, Angle, Eddy, Ehlers, Gibbard and Hughes2011; Fig. 1A and B). This retreat was punctuated by reversals and still stands marked by terminal moraines (Fig. 1C). (All radiocarbon dates are calibrated with IntCal20 [Reimer et al., Reference Reimer, Austin, Bard, Bayliss, Blackwell, Bronk Ramsey and Buzin2020], and errors are reported at 2σ, which is now standard.)
This paper summarizes recent optically stimulated luminescence (OSL) dating of late Wisconsin delta sands exposed in lakeshore cliffs along the north shore of Lake Erie near Jacksonburg, Ontario, and discusses their relevance to the Wisconsin history of the eastern Great Lakes. The results indicate the need for a comprehensive OSL dating program (as well as further calibrated radiocarbon dating) to establish a reliable time framework for the Wisconsin history in the area.
Lake Erie Bluffs
The shore bluffs along the north shore of Lake Erie, stretch for 84 km from Port Stanley to Long Point (Fig. 2).
(A) Location of Sand Hills Park on Quaternary map of Norfolk County (modified from Barnett et al., Reference Barnett, Cowan and Henry1991), Red lines show the location of the main lake bluff sections. (B) Interpreted cross sections from Port Bruce to Erie point view (from Barnett, Reference Barnett1993).
In the western exposures, the bluffs expose three clay-silt diamicts (Port Stanley Till), interbedded with glacial lake sand, silt, and clay rhythmites (Fig. 2B, I). The diamicts slope gradually eastward beneath lake level, marking several retreats and advances of a glacier. The lowermost diamict at Plum Point, 15 km west of Port Stanley, contains reworked larch (Larix spp.) and spruce (Picea spp.) wood, which gave three dates of 31.9 ± 3, 31.4 ± 2.4 and 28.8 ± 3.2 ka (Dreimanis, 1958), which are maximum ages: the peat balls must be reworked from much older deposits, because the dates are older than the last glacial maximum (LGM) of the Erie Lobe.
To the east, a long section of predominantly glacial lake deposits has complex and disputable relationships (Fig. 2B, II). Immediately east of Port Burwell, a remnant of the top Port Stanley diamict is overlain by disturbed silt rhythmites and sandy rhythmites. Eastward, the silt rhythmites supposedly lens out into a continuous sandy section at Sand Hills Park, where sandy rhythmites interfinger with mud-rich diamicts (Barnett, Reference Barnett1993, Reference Barnett1998; Barnett and Karrow, Reference Barnett and Karrow2018). In these sands, very mixed transported fossil plant assemblage of tundra, boreal forest, and prairie must have lived originally hundreds, or even thousands, of kilometers apart (Warner and Barnett,Reference Warner and Barnett1986; Dyke, Reference Dyke2005), so that the mixed plant assemblage must come from reworking of several successive stratigraphic horizons deposited during climate changes (Karrow and Warner, Reference Karrow, Warner, Laub, Miller and Steadman1988). Overlying dune sands are capped by a sandy forest luvisol (Barnett, Reference Barnett1998; Oakes, Reference Oakes2002). The massive diamict in this section is identified as Wentworth Till and the buried moraine as an extension of the Pairs/Galt moraine (Monaghan and Hansel, Reference Monaghan and Hansel1990; Karrow et al., Reference Karrow, Dreimanis and Barnett2000).
In the easternmost section between Turkey Point and Port Dover (Fig. 2B, III), sand rhythmites overlying diamict contain lenses of silty clay diamict dropped from icebergs; silty clays with ice-rafted clasts testify to a nearby ice front to the east (Barnett, Reference Barnett1993).
There are two alternative explanations of these sections.
The first is that the Sand Hills delta bottomset and foreset rhythmites pass eastward under and between the diamicts (Fig. 3A), with the lake delta marginal to a moraine (correlated with the Paris/Galt moraine to the northeast) fronting a glacier advancing into a lake (Fig. 3B). The youngest age of 16.5 ± 1.0 ka from supposed correlative sands at Vanderven to the west is comparable with the age of the Paris/Galt moraine, which is currently assigned to the Mackinaw interstadial standstill around 17 ka, but may be younger based on a date of 13.3 ± 0.5 ka from wood in lake silts resting on the moraine (Karrow, Reference Karrow1963; Monaghan and Hansel, Reference Monaghan and Hansel1990; Karrow et al., Reference Karrow, Dreimanis and Barnett2000). In that case, the delta was the terminus of outwash from that moraine.
(A) Stratigraphic relationships from Port Bruce to Port Dover on contemporary delta-diamict interpretation (after fig. 8 in Barnett and Karrow, Reference Barnett and Karrow2018). (B) Modern analogy: ice-marginal sedimentation in large ice-contact glacier-fed lake (Fig. 15 in Barnett and Karrow, Reference Barnett and Karrow2018).
The second interpretation is that the delta fills a valley cut into the moraine with younger flow diamicts from the eroding older moraine interfingering with the delta deposits: the valley cut and delta fill is younger than the moraine (Fig. 4A) and comparable to some South American glacial lake examples (Fig. 4B and C). In both cases, the upper topset beds are comparable to the adjacent Long Point bar complex (Fig. 4D and E).
(A) Interpreted stratigraphic interpretation on valley fill interpretation (from Zeman, Reference Zeman1980). (B and C) Modern analogy: older moraine, raised delta, and sandur relationships, Patagonian mountain lake (courtesy of J. Bendle). (D) Aerial view of Long Point, Lake Erie. (E) Well-sorted beach and bar sands, Long Point.
We prefer the valley fill interpretation based on the following observations.
In the Sand Hills sections, westerly flowing silty sand rhythmites within and below the diamicts fit better as subaqueous outwash from the glacier rather than part of the delta (sections SH-1 to LP-339; Fig. 5).
Details of central Sand Hills: measured sections LP85-4 to LP339, facies interpretations, and sample locations and optically stimulated luminescence (OSL) dates on LP85-4 Sand Hills Park (from Oakes [2002], with some sections from Barnett [1993]). Paleocurrents from Barnett and Karrow (Reference Barnett and Karrow2018).
Ice-rafted material, like that found in the rhythmites behind the Sand Hills diamicts, is not found in the delta rhythmites, as it should be if it was adjacent to an ice front in a lake that was calving icebergs (Fig. 2B, III).
There is a 15 km gap between the northeast-trending Sand Hills moraine and the north-trending Galt moraine north of Simcoe town, and the two moraine ridges are at right angles (Barnett et al., Reference Barnett, Cowan and Henry1991; Barnett, Reference Barnett1998; Barnett and Zilans, Reference Barnett and Zilans1998; Fig. 2A).
The Sand Hills diamict is a clayey silt to silty clay clast-poor till and is substantially finer than the Wentworth Till in the Galt moraine in the Brantford and Simcoe areas to the northeast, which is a sandy to silty sand clast-rich diamict formed of reworked subaerial outwash (Cowan, Reference Cowan1975; Barnett,1993; Arnaud et al., Reference Arnaud, McGill, Trapp and Smith2017). The Sand Hills diamict is practically identical to the silty clay clast-poor Port Stanley Till exposed to the west (Dreimanis and Barnett, Reference Dreimanis and Barnett1985).
On the valley fill interpretation, the Sand Hills sections outline an ice-marginal moraine on the east that was then cut into by a valley subsequently filled with flow tills interfingering with a lake delta with a different source building out from the north (Smith and Ashley, Reference Smith, Ashley, Ashley, Shaw and Smith1985; Fig. 5). The coarsening upward and mixed plant remains suggest either dropping lake level during deglaciation and opening of a lake outlet or sedimentation overwhelming rising lake level during a glacial advance and outlet blocking.
The only direct evidence of age for the Sand Hills delta comes from a cross-bedded sand at Vanderven, 5 km to the west of Sand Hills Park, which is correlated with the top sands of the Jackson delta (Barnett, Reference Barnett1998; Fig. 1A). Plant remains in this sand gave dates (2σ errors) of 30 ± 1.4 ka for several small pieces of wood and 13.6 ± 0.44 ka for Dryas intergrifolia leaves, a common species of arctic perennial (Dyck, Reference Dyck1967). The younger date from the arctic leaves is preferred, because the rounded wood fragments indicate abrasion and possible reworking, and leaves are much more easily destroyed than wood. But, the trough cross-bedded sands at Vanderven cut down into the underlying delta sand rhythmites and are coarser and better sorted (Barnett, Reference Barnett1998) and may be a younger outwash than the delta rhythmites.
To better define the ages of the Jackson delta at Sand Hills, we performed OSL dating on the sands at Sand Hills Park.
Although some of the silty finer-grained silty sands, possibly partly derived from the moraine, may have only been partially exposed to light and partially bleached, the well-sorted sands of the delta forests and topsets were subject to long-distance intermittent transport, temporary storage in a braided stream environment, and reworking in a shallow lake environment before final deposition. At least in principle, these deposits should be suitable for OSL dating and give reliable results (Fuchs and Owen, Reference Fuchs and Owen2008; Thrasher et al., Reference Thrasher, Mauz, Chiverrell and Lang2009)
METHODS
Sampling
Samples were taken upward from sand layers at section LP85-4, closest to the feather edge of the moraine (Fig. 4). A sediment surface at right angles to bedding was scraped back about 5 to 10 cm to expose fresher material. A wad of cotton wool was placed in the sediment-contact end of a 20 × 3 cm steel tube, and the tube was hammered into the sediment until the cotton wad appeared at the other end. The tube was then removed, a further cotton wool wad was put in the steel tube to prevent sediment mixing during transport, and the tube was wrapped longitudinally with at least five thicknesses of opaque duct tape to prevent light infiltration.
OSL analysis
The steel sample tubes were opened under subdued orange light (Sohbati et al., Reference Sohbati, Murray, Lindvold, Buylaert and Jain2017). The outer 2–3 cm were retained for radionuclide analysis (see below). The inner portion was wet sieved to recover the 180–250 μm grain-size fraction. This fraction was treated with 10% HCl and 10% H2O2 to remove carbonate and finely disseminated organics, respectively, followed by 10% HF to clean the sand grains and remove any surface-bound clays. The clean grains were density separated using a 2.58 g/mL aqueous heavy liquid (LST Fastfloat TM) to float off a K-rich feldspar fraction from the denser quartz-rich fraction. The quartz-rich fraction was then placed in 40% HF to remove any residual feldspar. The surface of the quartz grains was also etched in this step, removing the alpha-irradiated outer layer of quartz. Finally, the quartz grains were washed in 10% HCl for 1 h.
Radionuclide analysis for dose-rate calculation was performed using high-resolution gamma spectrometry (Murray et al., Reference Murray, Marten, Johnston and Martin1987, Reference Murray, Helsted, Autzen, Jain and Buylaert2018). The outer material from the sample tube was air dried and homogenized using a ring-grinder before being cast in wax in a disk-shaped geometry. Samples were counted for 24 h, after 21 d of storage to allow for secular equilibrium to be established between 222Rn (t ½ = 3.8 d) and its parent 226Ra. The radionuclide concentrations and the dry beta and gamma dose rates derived using conversion factors from Guérin et al. (Reference Guérin, Mercier and Adamiec2011) are given in Table 1. Bearing in mind the age of these samples (discussed later), one can safely assume that 226Ra is in equilibrium with its parent, and so we use the activity concentrations of 226Ra in dosimetry calculations.
Radionuclide concentrations and dry beta and gamma dose rates.a
a Uncertainties represent 2σ.
Total quartz and feldspar dose rates were calculated using a lifetime average water content estimated at 10% (the site is well drained). The K-feldspar dose rate includes an internal beta dose rate from 40K, assuming that the feldspar grains contain 12.5% K (Huntley and Baril, Reference Huntley and Baril1997). A small internal dose rate from U-Th of 0.02 ± 0.01 Gy/ka and 0.10 ± 0.05 Gy/ka for quartz and K-feldspar, respectively, is also incorporated (Zhao and Li, Reference Zhao and Li2005; Vandenberghe et al., Reference Vandenberghe, De Corte, Buylaert, Kučera and Van den haute2008). Cosmic ray dose rates were calculated based on Prescott and Hutton (Reference Prescott and Hutton1994)
Multigrain quartz (8-mm-diameter) and K-feldspar (2-mm-diameter) aliquots were prepared on stainless steel disks and cups, respectively, using silicone spray as an adhesive. All luminescence measurements were carried out on automated Risø thermoluminescence (TL)/OSL readers equipped with blue and IR diodes and a calibrated beta source. Because the quartz extracts showed weak infrared stimulated luminescence (IRSL) signals even after repeated etching, the quartz equivalent dose (D e) values were measured using a “double single-aliquot regenerative-dose” (SAR) protocol (Banerjee et al., Reference Banerjee, Murray, Bøtter-Jensen and Lang2001) in which each blue stimulation at 125°C (40 s) is preceded by an IR stimulation at 60°C (100 s). The preheat settings were 260°C for 10 s for the natural and regenerative dose signals and 220°C with immediate cooling for the test dose signals. Because all samples showed strong contributions from medium and slower components (even for aliquots where IRSL was negligible), an early background subtraction was used to maximize the contribution of the fast component, so that the net signal is derived from the first 0.32 s of the decay curve minus the subsequent 0.32 s. This inevitably led to weak signals, and aliquots that had an error of >10% on the natural test dose signal were rejected (59 out of 232 analyzed in total). To test the performance of our chosen SAR protocol, a dose-recovery test was carried out on six quartz aliquots of all samples (except sample 174207, because of insufficient material). The average dose-recovery ratio is 1.06 ± 0.06 (n = 40); two aliquots yielded given dose signals above the laboratory dose response curve and were rejected. Despite the large scatter in the data, we consider the performance of our SAR protocol satisfactory. Finally, between 30 and 47 equivalent doses were measured for each sample (except 174207). In addition to rejection based on signal strength, an interquartile range (IQR) criterion (Medialdea et al., Reference Medialdea, Thomsen, Murray and Benito2014) was used to reject outliers from the D e distributions; equivalent dose values that were lower than Q1 − 1.5 × IQR or higher than Q3 + 1.5 × IQR were rejected. This led to a further rejection of 11 aliquots. The average quartz D e values (±SE) and quartz OSL ages are given in Table 2.
Laboratory and field codes, sampling depth, water content (% dry water/dry weight sediment), equivalent dose (D e) values (K-feldspar and quartz), total dose rates, and uncorrected ages.a
a All uncertainties are 2σ. WC, water content; nR and nA, number of aliquots rejected and accepted, respectively, based on whether the response to the test dose has greater or less than 10% uncertainty; OSDL, optically stimulated light dosimetry. An asterisk (*) indicates no result.
K-feldspar IR50 and pIRIR290 D e values were measured using a standard pIRIR50/290 protocol (Buylaert et al., Reference Buylaert, Jain, Murray, Thomsen, Thiel and Sohbati2012); because the feldspar ages are only used to check the completeness of bleaching of the quartz OSL signal, no further performance tests were carried out (Murray et al., Reference Murray, Thomsen, Masuda, Buylaert and Jain2012; Table 2).
RESULTS
Seven of the eight samples gave satisfactory results (Table 2). A comparison of the quartz OSL with the available IR50 ages suggests that the quartz OSL signals of most of the samples were sufficiently bleached at deposition (using the criteria discussed in Murray et al. [2012] and Möller and Murray [Reference Möller and Murray2015]).The quartz OSL ages of the five delta samples (17ER02–17ER05, 17ER09) yield an overall age of 24.2 ± 1.3 ka (random uncertainty only); although the two older ages, 17ER03 and 17ER09, are from finer silty sands and may not have been completely bleached. The younger three (17ER02, 17ER09 and, 17ER04) young upward from 23.5 ± 1.7 to 23 ± 2 to 20.4 ± 1.8 ka and are consistent with the delta taking about 3 ka to form. The overlying dune sand and organic sandy soil samples (17ER06 and 17ER07) yield very young ages of ~240 and ~140 years that are in stratigraphic order and date modern dune formation.
Our average OSL age of 24.2 ± 1.3 ka, or the 23.5 to 20.4 ka range for the Jackson delta, is older than the age of 16.5 ± 1.0 ka for leaves of the arctic perennial Dryas intergrifolia leaves from the Vanderven sands to the west. This date correlates with the glacial retreat of the Mackinaw phase around 16.45 ± 260 ka (Monaghan and Hansel, Reference Monaghan and Hansel1990) to which age the Jackson delta was assigned by Barnett and Karrow (Reference Barnett and Karrow2018).
DISCUSSION
A sediment cannot be any older than its youngest constituent, though it can be younger.
The ~23.5 to 20.5 ka age of the Jackson delta slightly postdates the Nissouri phase (24.2 ka), during the interstadial lake-level rise of the Erie phase (Mörner, Reference Mörner1971; Karrow et al., Reference Karrow, Dreimanis and Barnett2000; Fig. 6). Reworked wood in the Catfish Creek Till, on which the Nissouri phase is based, gives ages (2σ errors) from 29.4 ± 3.0 to 28.9 ± 3.2 (data from Dreimanis et al., Reference Dreimanis, Terasmae and McKenzie1966). The Sand Hills delta and underlying diamicts are older than, and east of, the Port Bruce maximum advance and must therefore have been overridden by this advance at 18 ka. Though no diamict of this age is present at Sand Hills, the highly deformed rhythmites just above the Stanley diamict at the McConnell Nursery sections to the west may belong to this advance (Barnett, Reference Barnett1993, Reference Barnett1998). If 16.5 ± 1.0 ka for the Vanderven fluvioglacial sand is accurate, then their preservation fits with the relatively small lake-level rise and hence the rise in base level from lower to middle Lake Maumee (~16.5 ka) (Kincare and Larson, Reference Kincare, Larson, Schaetzl, Darden and Brandt2009). New OSL ages. however, suggest a short time of ~1 ka (16.9–15.9 ka) for formation of Lakes Maumee, Arkona, and Whittlesey (Fisher et al., Reference Fisher, Blockland, Anderson, Krantz, Stierman and Goble2015). So it is not possible to assign the Vanderven sediments to a specific lake. The oldest Dryas is now dated at 15.5 to 14.5 ka (Stuiver et al., Reference Stuiver, Grootes and Braziunas1995), and the Vanderven sand would thus fit in with rising lake levels as the oldest Dryas advance started blocking St. Lawrence drainage.
Inferred late Wisconsin stratigraphy of a south to north transect from Ohio to James Bay with youngest Sand Hills delta optically stimulated luminescence (OSL) date range and calibrated Vanderven (seds = sediments) radiocarbon dates. Uncalibrated radiocarbon timescale from Karrow et al. (Reference Karrow, Dreimanis and Barnett2000), calibrated with IntCal 2000 (Reimer et al., Reference Reimer, Austin, Bard, Bayliss, Blackwell, Bronk Ramsey and Buzin2020).
Recent studies on marine cores from the North Atlantic region (Bond et al. Reference Bond, Broecker, Johnsen, McManus, Labeyrie, Jouzel and Bonani1993; Bond and Lotti, Reference Bond and Lotti1995) and on ice cores from Greenland (Dansgaard et al., Reference Dansgaard, Johnsen, Clausen, Dahl-Jensen, Gundestrup, Hammer and Hvidberg1993; Andersen et al., Reference Andersen, Azuma, Barnola, Bigler, Biscayne, Caillon and Chappellaz2004; Capron et al., Reference Capron, Rasmussen, Popp, Erhardt, Fischer, Landais and Pedro2021) have highlighted drastic climatic changes of very short duration during the late glacial. The Sand Hills delta (~23.5–20.5 ka) is in the central part of Marine Isotope Stage 2 (MIS 2; 29–14 ka), shortly after the maximum ice coverage of the Laurentian ice sheets at ~24 ka (Dalton et al., Reference Dalton, Stokes and Batchelor2022) within the LGM (26.5–19.0 ka) (Clark et al., Reference Clark, Dyke, Shakun, Carlson, Clark, Wohlfarth, Mitrovica, Hostetler and McCabe2009; Fig. 7). The delta can be plausibly interpreted as having been deposited during rising lake level as the Erie Lobe advanced, blocking eastward drainage that eroded the valley.
Tentative recalibration of Lake Erie late Wisconsin events with Greenland ice core stratigraphy (from Leland McInnes, 2009: https://commons.wikimedia.org/wiki/File:Ice-core-isotope.png). Oxygen isotope boundaries from Lisiecki and Raymo (Reference Lisiecki and Raymo2005). European Dryas and Allerod-Bolling date assignments from Stuiver et al. (Reference Stuiver, Grootes and Braziunas1995). MIS, Marine Isotope Stage; NGRIP, North Greenland Ice Core Project.
CONCLUSIONS
The Jackson delta sands fill a valley cut into underlying ice front diamicts and associated subaqueous sediments. OSL dating of the Jackson delta sands at Sand Hills give consistent ages of 23.5 to 20.5 ka, indicating that the delta lasted for about 3 ka. This is 4 to 7 ka older than previously assigned based on lithologic correlation with calibrated radiocarbon-dated sediments 5 km to the west. It puts deposition of the Jackson delta in the Erie interstadial (possibly during ice advance during prolonged cooling after rapid early warming), after the LGM Nissouri stadial, and not in the fluctuating postglacial glacial retreat and rise in lake level of the Mackinaw phase, to which the younger fluvioglacial sediments at Vanderven to the west belong. But no coherent chronology of Great Lakes glacial history is possible without more accurate dating of many more sediments.
Acknowledgments
We greatly appreciate the comments of James Shulmeister on an earlier version of the paper. We also thank I. Peter Martini and the sadly late Steve Sadura for help in the field.
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