INTRODUCTION
Late Pleistocene and Holocene eolian dunes in the western Great Lakes region of North America (Fig. 1A) are increasingly being used as a source of evidence for paleolake levels, glaciofluvial sedimentation events, climate changes, and past atmospheric circulation patterns. A growing number of studies hypothesize causal links between coastal dune activity and lake level changes (e.g., Arbogast and Loope, Reference Arbogast and Loope1999; Loope and Arbogast, Reference Loope and Arbogast2000; Arbogast et al., Reference Arbogast, Hansen and Van Oort2002a, Reference Arbogast, Bigsby, DeVisser, Langley, Hanson, Daly and Young2010; Hansen et al., Reference Hansen, Arbogast, Packman and Hansen2003, Reference Hansen, Arbogast, van Dijk and Yurk2006, Reference Hansen, Fisher, Arbogast and Bateman2010; Blumer et al., Reference Blumer, Arbogast and Forman2012). Newly constructed inland dune chronologies have been recently utilized to infer eolian activity during the Pleistocene-Holocene transition and early Holocene (Arbogast et al., Reference Arbogast, Wintle and Packman2002b, Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015; Rawling et al., Reference Rawling, Hanson, Young and Attig2008; Loope et al., Reference Loope, Loope, Goble, Fisher, Jol and Seong2010; Miao et al., Reference Miao, Hanson, Wang and Young2010; Campbell et al., Reference Campbell, Fischer and Goble2011; Kilibarda and Blockland, Reference Kilibarda and Blockland2011; Loope et al., Reference Loope, Loope, Goble, Fisher, Lytle, Legg, Wysocki, Hansen and Young2012). Coastal spits and dunes have also been employed to reconstruct paleowind patterns associated with a hypothesized anticyclone, which may have persisted over a retreating Laurentide Ice Sheet (Krist and Schaetzl, Reference Krist and Schaetzl2001; Kilibarda and Blockland, Reference Kilibarda and Blockland2011; Vader et al., Reference Vader, Zeman, Schaetzl, Anderson, Walquist, Freiberger, Emmendorfer and Wang2012). Nearly all of these studies use optically stimulated luminescence (OSL) to estimate the age of eolian sediments as this method is well suited to quartz-dominated loess and dune sand.
(color online) (A) Location map of the western Great Lakes region of North America. (B) Location of the study area in Ottawa County, Michigan, and areas of inland dunes in Lower Michigan (shaded areas are after Arbogast and Jameson [Reference Arbogast and Jameson1998]). (C) Shaded relief image derived from a 2004 LIDAR (light detection and ranging) digital elevation model of Ottawa County, Michigan. Location of our two optically stimulated luminescence (OSL) sample sites at Hemlock Crossing Park (HC) and Pigeon Creek Park (PC). Previous radiocarbon and OSL dune studies at Rosy Mound Natural Area (RM) and Hoffmaster State Park (HM). Coastal dune sediment samples from Kirk Park (KP). Allendale delta sediment samples from near Allendale, Michigan (AD).
Two distinct populations of dunes have been recognized in Michigan as a result of previous studies: coastal dunes and inland dunes (Arbogast et al., Reference Arbogast, Scull, Schaetzl, Harrison, Jameson and Crozier1997; Arbogast and Jameson, Reference Arbogast and Jameson1998; Arbogast, Reference Arbogast2009). Coastal dunes are found along the shores of the western Great Lakes (Fig. 1B) and are primarily middle to late Holocene phenomena, related to coastal evolution and lake level changes following the Nipissing transgression (e.g., Arbogast and Loope, Reference Arbogast and Loope1999; Arbogast et al., Reference Arbogast, Hansen and Van Oort2002a, Reference Arbogast, Bigsby, DeVisser, Langley, Hanson, Daly and Young2010; Hansen et al., Reference Hansen, Fisher, Arbogast and Bateman2010). Coastal dunes are large parabolic dunes up to 50 m in relief, and sometimes perched up to 100 m above the current lake surface (Arbogast, Reference Arbogast2009). A back dune complex of lower-relief parabolic dunes and dune ridges is also present up to a few kilometers inland (e.g., Arbogast and Loope, Reference Arbogast and Loope1999; Arbogast et al., Reference Arbogast, Hansen and Van Oort2002a, Reference Arbogast, Bigsby, DeVisser, Langley, Hanson, Daly and Young2010; Hansen et al., Reference Hansen, Fisher, Arbogast and Bateman2010). Radiocarbon and OSL analyses for coastal dunes in Lower Michigan yield ages less than ~6.0 ka, although a few dunes have produced slightly older ages (Hansen et al., Reference Hansen, Fisher, Arbogast and Bateman2010).
Dunes are also found on abandoned outwash and lacustrine plains, well inland from coastal dunes (Fig. 1B). Inland dunes have much lower relief (~10 m) than coastal dunes and are part of extensive sand sheets, which cover abandoned outwash and lacustrine plains (e.g., Arbogast et al., Reference Arbogast, Scull, Schaetzl, Harrison, Jameson and Crozier1997, Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015; Arbogast and Jameson, Reference Arbogast and Jameson1998; Loope et al., Reference Loope, Loope, Goble, Fisher, Jol and Seong2010, Reference Loope, Loope, Goble, Fisher, Lytle, Legg, Wysocki, Hansen and Young2012). Only three OSL studies estimate the age of inland dunes on abandoned outwash and glacial lacustrine plains in Michigan, and these studies have produced late Pleistocene and early Holocene ages for these dunes (Loope et al., Reference Loope, Loope, Goble, Fisher, Jol and Seong2010, Reference Loope, Loope, Goble, Fisher, Lytle, Legg, Wysocki, Hansen and Young2012; Arbogast et al., Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015). Notably, there are no OSL studies for inland dunes found on the former bed of Glacial Lake Chicago in western Lower Michigan (Fig. 1B), even though inland dunes are common in this area and cover an estimated area greater than 200 km2 in Ottawa County, Michigan, alone (Fig. 1C).
In this article, we present the first OSL ages for inland dunes on the abandoned bed of Glacial Lake Chicago in western Lower Michigan (Fig. 1C). Our new ages demonstrate that these inland dunes were active during the latest part of the Bølling-Allerød and the subsequent Younger Dryas and Preboreal events immediately following final drainage of Glacial Lake Chicago after ~13.6 ka (Larson, Reference Larson2011). Our OSL ages add to a growing number of OSL studies of inland dune fields in the western Great Lakes region and demonstrate a peak in eolian activity during, and slightly after, the end of the Younger Dryas event. Additionally, all of these studies demonstrate northwesterly or westerly winds and do not support the hypothesis of easterly anticyclonic winds along the retreating ice margin of the Laurentide Ice Sheet during the Pleistocene to Holocene transition.
Geomorphic setting of inland dunes
Landforms and sediments in Ottawa County, Michigan, are predominately late Pleistocene glaciolacustrine plains of gravelly nearshore sand, moraines and till plains composed of silt-rich diamicton, and valley trains of sand and gravel between end moraines (Fig. 2). Wisconsin Episode (formerly late Wisconsinan) and older glaciogenic sediments vary from ~10 to >100 m thick and cover late Mississippian bedrock of shale, sandstone, and limestone (Colgan et al., Reference Colgan, Vanderlip and Braunschneider2015). In eastern Ottawa County, there are end moraines, till plains, uplands, and associated valley trains of the Valparaiso and Lake Border moraine systems (Fig. 2) formed during the Crown Point Phase ~18,200 to 16,800 cal yr BP (Leverett and Taylor, Reference Leverett and Taylor1915; Curry et al., Reference Curry, Grimley and McKay2011; Larson, Reference Larson2011). The western half of Ottawa County is a sandy lacustrine plain abandoned by Glacial Lake Chicago after ~13,600 yr BP (Larson, Reference Larson2011) and subsequently modified by eolian, fluvial, and coastal processes (Figs. 1C and 2).
(color online) (A) Map of soil textures of parent materials in Ottawa County. Sand textured soils are shown in yellow, and loam textured soils are shown in green (data are from the US Department of Agriculture’s SSURGO Database--https://www.nrcs.usda.gov/wps/portal/nrcs/detail/soils/survey/?cid=nrcs142p2_053627, accessed March 1, 2016). (B) Landforms of Ottawa County, Michigan. Gray areas are end moraines and till plains of the Lake Border (LBM) and Valparaiso (VM) moraine systems, which were deposited by the Lake Michigan lobe as it advanced out of Lake Michigan basin and flowed to the east and southeast (distal sides of moraines are on the east). Thick dark lines are moraine ridge crests. Thin black lines are inland dune crests, and thin gray lines are coastal dune crests. Allendale delta (AD) and Zeeland delta (ZD) sediments are shown in stippled pattern. (C) The highest shoreline of Glacial Lake Chicago during the Glenwood I and II levels is shown with a dark line based on the descriptions of Leverett and Taylor (Reference Leverett and Taylor1915), and highest elevations of the Allendale (~204 m amsl) and Zeeland (~202 m amsl) deltas. (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.)
Inland dunes on the abandoned bed of Glacial Lake Chicago are covered in forest where not disturbed or heavily modified by humans. Before European settlement in the early 1800s, the area around Pigeon River in western Ottawa County (Fig. 3A) was composed of sandy uplands, covered by a dry-mesic northern forest of Pinus strobus, Quercus albus, Quercus rubra, Acer rubrum, Fagus grandifolia, Prunus serotina, Populus grandidentata, and Tsuga canadensis. The river valleys were dominated by marsh, wet meadows, floodplain forests, and hardwood conifer swamps (William Martinus & Associates, 2000). Most of the inland dunes in Ottawa County show evidence of wind reworking and human disturbance. Small blowouts in the dunes indicate deflation following intensive logging in the nineteenth century. Heavily disturbed dune areas were planted with Pinus resinosa by the Civilian Conservation Corp in the 1930s (William Martinus & Associates, 2000). These eroded, inland dune sites are easy to identify because soil profiles are absent in blowouts, and downwind areas are buried in eroded soils, which commonly bury preserved soil profiles.
(color online) (A) Map showing sampling sites for optically stimulated luminescence (OSL) and radiocarbon analyses. Hemlock Crossing County Park (HC) and Pigeon Creek County Park (PC). (B) Hemlock Crossing OSL site (42°55.2624' N; 86°9.1608' W; World Geodetic System of 1984 [WGS 84]). (C) Pigeon Creek Park OSL site (42°55.9110' N; 86° 5.5494' W; WGS84=World Geodetic System of 1984). OSL sample sites are shown with black circles, and radiocarbon samples from vibracores in alluvial are shown with black squares. “T” indicates Lake Nipissing age terraces along the Pigeon River.
Glacial and postglacial lakes of the Lake Michigan basin
Glacial Lake Chicago occupied the Lake Michigan basin between ~17,000 and ~13,600 cal yr BP (Table 1, Fig. 2C) based on the existing calibrated radiocarbon chronology (Larson and Schaetzl, Reference Larson and Schaetzl2001; Kincare and Larson, Reference Kincare and Larson2009; Curry et al., Reference Curry, Grimley and McKay2011; Larson, Reference Larson2011). At its highest levels (Glenwood and Calumet Phases), Glacial Lake Chicago drained southward through an outlet near Chicago into the Mississippi drainage basin (Bretz, Reference Bretz1951). The historical mean level of modern Lake Michigan is ~176.6 m above mean sea level (amsl). Glacial Lake Chicago rose to a maximum level of between 202 and 204 m amsl in the study area (Fig. 2C) based on the highest elevations of the Allendale and Zeeland deltas (Fig. 2C) as mapped by Leverett and Taylor (Reference Leverett and Taylor1915). The Glenwood I level (Table 1) occurred during and after the retreat of the Lake Michigan lobe following the Crown Point Phase after ~17,000 cal yr BP (Curry et al., Reference Curry, Grimley and McKay2011; Larson, Reference Larson2011). The Mackinaw Phase (~16,500 to 15,800 cal yr BP) marked a period of low lake level when ice retreated north opening a spillway in the Straits of Mackinaw (Hansel et al., Reference Hansel, Mickelson, Schneider and Larsen1985; Hansel and Mickelson, Reference Hansel and Mickelson1988). The Lake Michigan lobe then readvanced during the Port Huron Phase (~15,800 to 15,200 cal yr BP) as far south as Grand Haven, Michigan, and causing Glacial Lake Chicago to rise again to the Glenwood II level (Larson, Reference Larson2011). The Calumet level of Glacial Lake Chicago (Table 1) occurred during the Two Rivers Phase ~15,200 to ~13,600 cal yr BP (Larson, Reference Larson2011). After ~13,600 cal yr BP, Glacial Lake Chicago ceased to exist as ice retreated north and the lake merged with early Glacial Lake Algonquin to form the larger main Algonquin Phase at a level probably lower than the present lake level in the study area (Larson, Reference Larson2011).
Glacial and postglacial lake levels in the Lake Michigan basin.
a Our estimates of lake level elevations for Ottawa County based on sediments and landforms. amsl, above mean sea level.
b Age estimates for lake levels are from Kincare and Larson (Reference Kincare and Larson2009), Larson (Reference Larson2011), and Baedke and Thompson (Reference Baedke and Thompson2000). Age range is possible time of lake level.
c There is no evidence for these lakes in Ottawa County as both levels are thought to have been lower than current level of Lake Michigan (Kincare, Reference Kincare2007).
d The final phase of Glacial Lake Chicago (Calumet level) occurred after the Two Rivers–Onaway Phase estimated by Larson (Reference Larson2011) as occurring at ~11,700 14C yr BP (~13,600±150 cal yr BP).
Following Glacial Lake Algonquin, postglacial Lake Chippewa formed at a much lower level (as low as ~70–90 m amsl) because of opening of drainage paths to the north and east (Larson and Schaetzl, Reference Larson and Schaetzl2001; Kincare, Reference Kincare2007). The lowest level of Lake Chippewa is thought to have occurred at ~11,000 cal yr BP (Kincare, Reference Kincare2007). As a result of this large drop in lake level, rivers in western Michigan incised deeply in response to lowered base levels (Kincare, Reference Kincare2007). The Grand, Pigeon, and Macatawa Rivers all have morphologies and valley fills consistent with this hypothesis. Lake level then rose gradually because of rebound of the outlet of Lake Chippewa to the north and east, finally reaching high stands of Lake Nipissing at ~5500 and ~4500 cal yr BP (Baedke and Thompson, Reference Baedke and Thompson2000). Lake Nipissing probably reached its highest elevation in the study area of ~186 to 187 m maslbased on a prominent wave-cut cliff near Holland, Michigan, and well-developed stream terraces along the Grand, Pigeon, and Macatawa Rivers.
Previous dune research in western Michigan
Coastal dunes have been well studied in and adjacent to Ottawa County, Michigan. Arbogast and Loope (Reference Arbogast and Loope1999) examined coastal dunes at Rosy Mound Natural Area (Fig. 1C) in northwestern Ottawa County as part of a larger study of dunes along the eastern shoreline of Lake Michigan. They provided the first radiocarbon ages of buried soils to demonstrate that coastal dunes are post-Nipissing features younger than ~6000 cal yr BP. Coastal dunes have also been studied just south of Holland, Michigan, in northwestern Allegan County, and at P.J. Hoffmaster State Park (Fig. 1C) in northwestern Ottawa County and southwestern Muskegon County (Loope and Arbogast, Reference Loope and Arbogast2000; Arbogast et al., Reference Arbogast, Hansen and Van Oort2002a; Hansen et al., Reference Hansen, Arbogast, Packman and Hansen2003, Reference Hansen, Arbogast, van Dijk and Yurk2006, Reference Hansen, Fisher, Arbogast and Bateman2010). The Holland dune complex contains active and inactive parabolic dunes up to 50 m high, and lower-relief inactive back dune ridges. These dunes produced calibrated radiocarbon and OSL ages varying from ~0.3 to 5.9 ka (Hansen et al., Reference Hansen, Fisher, Arbogast and Bateman2010). The dune complex at Hoffmaster State Park (Fig. 1C) has a more varied assemblage of dune types with several overlapping generations of large active and inactive parabolic dunes, and several generations of overlapping back dune ridges (Hansen et al., Reference Hansen, Fisher, Arbogast and Bateman2010). OSL ages for these dunes produced ages from ~0.3 to ~7.2 ka (Hansen et al., Reference Hansen, Fisher, Arbogast and Bateman2010). Interestingly, the oldest OSL age at Hoffmaster State Park (7.2±1.0 ka) was from a back dune ridge about 1 km inland from Lake Michigan. Another anomalously old OSL age (10.5±1.4 ka) was reported from a large parabolic dune in Warren Dunes State Park, Indiana (Hansen et al., Reference Hansen, Fisher, Arbogast and Bateman2010). Both of these ages suggest that pre-Nipissing age dunes may have been reworked and later buried during the late Holocene. These previous studies confirm that coastal dunes in the study area are Nipissing or younger in age (<6 ka). None of these previous studies discuss or provide ages for the small inland dunes that we focus on in this article.
MATERIALS AND METHODS
We carefully selected our two inland dune OSL sampling sites (Figs. 3 and 4) based on them having a preserved dune crest and soil profiles suggesting long-term stability. Finding suitable OSL sampling sites was facilitated by use of a digital elevation model (DEM) derived from LIDAR (light detection and ranging) data collected by Ottawa County, Michigan, in 2004. The DEM has a horizontal resolution of ~3 m and a vertical accuracy of ~0.1 m. The DEM greatly enhanced our ability to pick suitable OSL sampling sites that were not eroded or reworked. Both of the dunes we sampled have preserved dune crests with gentle windward sides and steeper lee sides (Figs. 3 and 4). The sample sites are covered in forest. Most importantly, both dune crests have well-developed O/A/E/B horizons with sesquioxides and translocated humus (Bhs)/C soil horizons with sola depths of ~60 to 70 cm developed on their dune crests (Figs. 5 and 6). Additionally, ground-penetrating radar (GPR) profiles run across the dune crest at the Pigeon Creek OSL sampling site indicate eastward-dipping slip faces in the dune (Fig. 7). The preserved soil profiles, history of forest cover during the Holocene, and eastward-dipping slip faces in a GPR profiles, suggest that our OSL sampling sites have been stable during the Holocene.
Topographic profiles of dune sample sites at Pigeon Creek Park (A) and Hemlock Crossing Park (B). Profiles run across the dune crest where soil pits for optically stimulated luminescence samples were dug (black bars). Note that the total relief of each dune is less than 10 m. Vertical exaggeration is ~3.3:1 in both profiles. The dashed boxes are approximate coverages of the two ground-penetrating radar profiles shown in Figure 7.
(color online) Photographs of the dune sampling sites and soil pits. (A) Hemlock Crossing sampling site looking to the southwest along the crest of the dune. The leeward side of the dune is to the left, and the windward side is to the right. (B) Soil pit at Hemlock Crossing Park site (northwest pit wall). (C) Pigeon Creek sampling site looking to the southeast; the leeward side of the dune is visible in the background sloping to the east. (D) Soil pit and profile at Pigeon Creek Park (north pit wall). The soil master horizons are labeled with A, E, B, and C.
(color online) Graphic soil profiles from Hemlock Crossing and Pigeon Creek Parks on dune crest optically stimulated luminescence (OSL) sampling sites. Both soils are weakly developed Spodosols. Black dots indicate depths where OSL samples were taken. Bhs, B horizons with sesquioxides and translocated humus.
(color online) Ground-penetrating radar (GPR) reflection profiles of the inland dune at Pigeon Creek County Park. These profiles run west to east, the same as the dune profile in Figure 4A. The profile was obtained using a PulseEkko 100 system. A common midpoint offset survey estimated wave velocity of 0.132 m/ns for the dune sand at the site. (A) GPR profile across dune crest using a 50 MHz frequency antennae with a transmitter receiver separation of 2 m, step size of 0.5 m, and stacking of 128 times; total length of profile is 60 m, and total depth is ~20 m. (B) Our interpretation of the profile in panel A. Red dashed lines mark the interpreted contact of the dune sediment with underlying Glacial Lake Chicago nearshore sediment (highest dashed line) and the groundwater table (lowest dashed line). (C) GPR profile obtained with a 100 MHz frequency antennae with a transmitter receiver separation of 1 m, step size of 0.25 m, and stacking of 128 times; total length of profile is 25 m, and total depth is ~17 m. (D) Our interpretations of buried slip faces in the dune (red solid lines). Interpretations of sediment and groundwater table are the same as in panel B. (For interpretation of the references to color in this figure legend, the reader is referred to the web version of this article.)
Samples for OSL dating were collected in soil pits roughly 1.5 m × 1.5 m and 1.7 m deep (Fig. 5). All of our OSL samples were taken from below 1.2 m depth, below the sola depth and root zone that extends to ~0.6–0.7 m. Aluminum sample tubes were driven into the pit wall and then carefully excavated. Tube ends were packed with Styrofoam to avoid sample movement during transport. One sample (HC-3) was collected below the bottom of the pit using a bucket auger, ~10 cm in diameter, in order to obtain a deeper sample (~2.45 m depth). A sample tube was then driven into the bucket of the auger and then treated as described previously. Samples for moisture content were collected from within ~20 cm of the tube samples. Soil profiles were described for horizon thickness, organic matter, texture, Munsell soil color, and any special characteristics (Buol et al., Reference Buol, Hole and McCraken1989). Sediment grain-size distributions were determined using dry-sieving methods (Lewis and McConchie, Reference Lewis and McConchie1994). We did not wash samples before sieving because they contained less than 1% fines (Table 2). Grain-size statistics were calculated using GRADISTAT v. 8.0 (Blott and Pye, Reference Blott and Pye2001). When citing ages, we use “ka” for all OSL age dates and “cal yr BP” for ages estimated using the radiocarbon method or the existing radiocarbon chronology.
Texture data for eolian and glaciolacustrine sediments in Ottawa and Muskegon Counties, Michigan.
Notes: gr=gravel; vcs=very coarse sand; cs=coarse sand; ms=medium sand; fs=fine sand; vfs=very fine sand.
a Sorting coefficient=D 90/D 10.
OSL laboratory methods
OSL analyses were performed at the Middlebury College Luminescence Laboratory. Full analytical details are available in the Supplementary Materials. All luminescence samples were processed under a 589 nm sodium vapor lamp further filtered with a Lee 101 filter. Following overnight treatments in 10% HCl and bleach, modal size fractions (165 to 250 µm) of each luminescence sample underwent multiple density separations in solutions of lithium heteropolytungstate to obtain a pure quartz fraction (ρ=2.58 to 2.66 g/mL). Quartz samples then underwent two 30-minute etches in concentrated HF before a final 30-minute etching in concentrated HCl. All samples were then hand-rubbed and resieved through an 80 μm cloth to break apart low-quality fragments and ensure measurement of intact, high-quality grains.
Signals were measured on small aliquots (~20 to 100 grains per disk) following the standard single aliquot regenerative (SAR) procedure (Murray and Wintle, Reference Murray and Wintle2000). Strict rejection criteria were applied, including 10% rejection thresholds for the recycling, recuperation, and test dose repeatability tests. Postanalysis IR checks were used to verify sample purity. Fast ratios suggest that shine-down curves were dominated by the fast component and a rejection threshold of aliquots with fast ratios less than 12 (Durcan and Duller, Reference Durcan and Duller2011). Early background correction was employed to further minimize the potential impact of slow and medium components (Cunningham and Wallinga, Reference Cunningham and Wallinga2010). This involved subtraction of the mean signal over the 4- to 5-second interval from the mean signal over the 0- to 0.5-second interval. Equivalent dose (D e ) for individual disks was estimated using a quadratic fit to all of the measured SAR steps. Burial dose for samples was estimated using the central age model, which is justified given that overdispersion was always <20%, skew was <1, and kurtosis was between −1 and 1 (Galbraith et al., Reference Galbraith, Roberts, Laslett, Yoshida and Olley1999).
Dose rates were calculated from the inductively coupled plasma mass spectrometry (ICP-MS) bulk geochemistry of representative samples collected within a 20 cm radius of each sample’s location (Guerin et al., Reference Guerin, Mercier and Adamiec2011). Chemical analyses were performed by ALS Minerals in Reno, Nevada, using a lithium metaborate fusion followed by ICP-MS analysis for both trace and major elements. Dose rates and ages were then computed using the online DRAC (dose rate and age calculator) v. 1.1 (Durcan et al., Reference Durcan, King and Duller2015). Water contents were computed on samples collected from a 20 cm sphere using a mass difference calculation after drying in an oven for 2 days at 60°C (wet weight − dry weight at room temperature).
RESULTS
Dune distribution, morphology, and sedimentology
Inland dunes in the study area occur as far as ~15 km inland from Lake Michigan (Figs. 1C and 3A). The highest elevation of the lacustrine plain on which inland dunes are developed is ~200 mamsl (~23 m above current level of Lake Michigan), and the lowest elevation is ~185 m amsl (~8 m above lake level). The highest inland dunes have a relief of ~10 m and vary from ~50 to 100 m wide with dune ridges commonly traceable for more than a kilometer (Fig. 3A). Inland dune morphologies are classified as compound and complex parabolic dunes (Cooke et al., Reference Cooke, Warren and Goudie1993). The dune sampled at Hemlock Crossing Park (Fig. 3B) is part of a compound parabolic dune with arms oriented to the northwest (~340°). The dune at Pigeon Creek is part of a rakelike compound parabolic dune that is oriented to winds coming from the west (Fig. 3C). Both of the inland dunes we sampled are part of an extensive sand sheet, and a series of imbricate ridges so must have formed and stabilized at roughly the same time (Fig. 3A).
The two inland dunes we sampled for OSL dating are composed of fine sand (Table 2) with a mean D 50 of 209±19 μm, and with fines much less than 1% (n=6, 2-sigma). Inland dune sand is significantly finer than coastal dune samples collected just west of our sites (Fig. 1C, site KP) on the crests of two large parabolic dunes at Kirk Park (D 50 of 270±28 μm, n=6). Sediments of the Allendale delta deposited in Glacial Lake Chicago in the area (Fig. 1C, site AD; Table 2) are composed of moderately to poorly sorted, gravelly medium sands with a mean D 50 of 294±17 μm (n=3). This and other lacustrine units cover large areas of Ottawa, Muskegon, Allegan, and other coastal counties in western Michigan. The sediment has been mapped and interpreted as nearshore lacustrine sand and gravel deposited during the Glenwood and Calumet levels of Glacial Lake Chicago (Leverett and Taylor, Reference Leverett and Taylor1915; Martin, Reference Martin1955; Farrand, Reference Farrand1982). The lacustrine sand and gravel varies from a few meters thick to well over 20 m thick based on mapping and water well records in Ottawa and Muskegon Counties. At depth, offshore silt and clay beds are commonly interbedded with or underlie the lacustrine sand and gravel (Colgan and Stark, Reference Colgan and Stark2005a, Reference Colgan and Stark2005b; Colgan and Tort, Reference Colgan and Tort2006; Colgan et al., Reference Colgan, Vanderlip and Braunschneider2015). Seven near-surface samples of Glacial Lake Chicago nearshore sediment collected in southeastern Muskegon County (Table 2) are moderately to poorly sorted, gravelly medium sand and have a D 50 of 307±26 μm (n=7).
No sedimentary structures or unconformities below the base of the sola were observed in either of the two soil pits dug during OSL sampling. Slip faces have been observed in sand pits in other inland dunes in the study area if the bedding is dried out and etched by winds, but it is very difficult to see these slip faces in fine eolian sand, especially when moist and in a small exposure such as a hand-dug soil pit. A GPR profile run across the dune through our sampling site at Pigeon Creek Park shows dipping reflectors that we interpret as slip faces (Fig. 7). Two other prominent reflectors at depth in the profiles are interpreted as the contact between dune sand and gravelly nearshore lacustrine sand, and the underlying water table (Fig. 7).
Soil profiles developed on inland dunes
Soil horizons are present on the inland dunes of western Ottawa County where they are not eroded by blowouts or heavily modified by humans. Many inland dunes are extensively modified by small blowouts that have completely eroded all soil horizons and left depressions from 1 to 5 m deep and from 10 to 50 m in diameter (Fig. 3B and C). Most of the inland dunes of Hemlock Crossing Park and Pigeon Creek Park are mapped as “blown out land” in the Soil Survey of Ottawa County, Michigan (US Department of Agriculture, Soil Conservation Service, 1972), even though preserved soils or buried soils are present in numerous locations. Where soils are preserved or buried by blown sand, soils probably correspond to those of the Rubicon Series. Soil profiles in these areas can be classified as Inceptisols or Spodosols with thin O, A, and E horizons over weak B horizons (Bw) or spodic horizons (Bhs) and sometimes contain ort stones developed in the upper part of the B horizon. Figure 6 shows the soil profiles described in the OSL sampling pits at Hemlock Crossing and Pigeon Creek Parks on dune crests. At both sample sites, the soil profiles on the dune crests were O/A/E/Bhs/BC/C, with total sola thickness of ~60 to 70 cm.
Radiocarbon ages of Pigeon River valley alluvium
Table 3 lists radiocarbon ages from buried organic beds in alluvium filling the Pigeon River valley. Four calibrated accelerator mass spectrometry (AMS) ages vary in age from 5910 to 6780 cal yr BP (2-sigma range for four ages; Colgan and Stevens, Reference Colgan and Stevens2016). These samples were collected in a series of vibracores taken across the valley and are from depths ranging from 2.5 to 2.8 m below the current floodplain surface (Fig. 3). An additional AMS radiocarbon age was obtained from alluvium sample in a vibracore recovered near the dune sample site at Pigeon Creek Park (Fig. 3). This wood sample is from a depth of 2.3 m and produced a 2-sigma calibrated age of 2345 to 2490 cal yr BP (Table 3).
Radiocarbon ages from the organic material in alluvium of the Pigeon River valley.
a All accelerator mass spectrometry samples pretreated with acid/alkali/acid washes.
b Radiocarbon calibration uses IntCal09.
OSL ages of dune sediments
Table 4 lists the OSL ages for the six dune samples taken from two sites. The ages (Fig. 8) are well clustered and range from 11.6±0.9 to 13.3±1.1 ka (2-sigma). The oldest OSL age is from a depth of 2.45 m, from the dune at Hemlock Crossing Park. The youngest OSL age is from Pigeon Creek Park from a depth of 1.50 m. All of the ages are within 2-sigma uncertainty of one another, although the mean age of sample HC-3 (13.3±1.1 ka) is slightly older than the other five samples (Fig. 6). Although not significant at the 2-sigma level, this is notable given that sample HC-3 is from a greater depth (2.45 m) than the other samples.
Plots showing ages of multiple aliquots for each sample (black dots), 2-sigma uncertainties (thin lines), and the summed probability distribution of all ages accepted for a given sample (dashed black line).
Optically stimulated luminescence analyses for dune samples from Hemlock Crossing and Pigeon Creek County Parks.
DISCUSSION
OSL ages of inland dunes in Ottawa County, Michigan
Our OSL ages from the two inland dunes (Table 4 and Fig. 8) are significantly older than previously published OSL and radiocarbon ages for middle to late Holocene coastal dunes in the study area (see Figs. 1 and 3A for location of coastal dunes in the study area). This indicates that inland dunes in the study area are not associated with the well-documented period of eolian activity in coastal Michigan that occurred following the fall from Nipissing high stand after ~5500 cal yr BP (e.g., Loope and Arbogast, Reference Loope and Arbogast2000; Arbogast et al., Reference Arbogast, Hansen and Van Oort2002a; Hansen et al., Reference Hansen, Arbogast, Packman and Hansen2003, Reference Hansen, Arbogast, van Dijk and Yurk2006, Reference Hansen, Fisher, Arbogast and Bateman2010). Alternatively, our OSL ages indicate that inland dunes in the study area formed during the Pleistocene-Holocene transition.
The soil profiles we describe corroborate our new OSL ages (Figs. 5 and 6). The soils developed on inland dune crests are weakly to moderately developed Spodosols similar to soils developed on lacustrine surfaces underlying the younger coastal dunes at Rosy Mound Natural Area (Arbogast and Loope, Reference Arbogast and Loope1999). This confirms that our two inland dunes are significantly older than coastal dunes, which are mid- to late Holocene age. Additionally, dunes and soil profiles similar to those in the study area have also been described in the Saginaw Lowland in east-central Lower Michigan (Fig. 1B) (Arbogast et al., Reference Arbogast, Scull, Schaetzl, Harrison, Jameson and Crozier1997; Arbogast and Jameson, Reference Arbogast and Jameson1998). Soils developed on these dunes are also Spodosols, or Inceptisols trending toward Spodosols. Dunes in the Saginaw dune field likely formed after the retreat from the Port Huron advance when Glacial Lake Saginaw drained and the lake bed was exposed (Arbogast et al., Reference Arbogast, Scull, Schaetzl, Harrison, Jameson and Crozier1997; Arbogast and Jameson, Reference Arbogast and Jameson1998). This history is very similar to what occurred in the study area.
Radiocarbon ages of Pigeon River valley fill provide additional corroborating evidence and demonstrate the stratigraphic consistency of our OSL ages. The radiocarbon ages are on buried wood and organics from wetland sediment buried ~2.3 to 2.8 m below the current floodplain. The calibrated AMS radiocarbon ages of buried organics in the alluvium in the Pigeon River valley vary from ~2345 to 6780 cal yr BP (Table 3) demonstrating that the valley was incised before 6780 cal yr BP (Colgan and Stevens, Reference Colgan and Stevens2016). Colgan and Stevens (Reference Colgan and Stevens2016) interpreted the valley fill sequence at Hemlock Crossing Park (Fig. 3) as indicating valley incision during the Chippewa low stand (~11,000 to 9000 cal yr BP), followed by transgression and valley aggradation from ~9000 to ~5500 cal yr BP. The buried alluvial organics formed in wetlands during the Lake Nipissing transgression. Because the inland dunes are crosscut by the valley, it is clear that the dunes are older as demonstrated by our new OSL ages. Fluvial terraces in the Pigeon River valley vary from ~3 to 10 m above the current level of Lake Michigan and were likely formed during and after the Nipissing transgression. These terraces truncate the inland dunes all along the valley indicating that the dunes are older than the Nipissing high stand (~5500 cal yr BP). If the dunes were younger, we would expect them to cover these terraces. On the other hand, large coastal dunes have migrated across the valley and partially blocked the mouth of Pigeon Lake, near Lake Michigan.
In summary, our OSL ages, soil profiles, radiocarbon ages, and stratigraphic position and geomorphic setting of inland dunes all demonstrate that inland dunes in the study area formed after the estimated time of drainage of Glacial Lake Chicago after ~13.6 ka and before the Nipissing transgression and high stand at ~5500 cal yr BP (Table 1). Based on the range of our OSL ages, dune activity probably began during the late Bølling-Allerød after ~13.6 ka and continued as late as the Preboreal event at ~11.5 ka. The peak of dune activity occurred during the Younger Dryas event.
Source of inland dune sand
The source of the inland dune sand must have been locally derived and deflated from the exposed bed of Glacial Lake Chicago, which is composed of poorly sorted, gravelly medium sand (Table 2). Inland dunes in the study area are dominated by fine sand, whereas the larger coastal dunes are dominated by medium sand (Table 2). Support for our hypothesis of deflation of exposed lake sediments is found in the availability of abundant fine sand in the sandy nearshore lacustrine sediments of Glacial Lake Chicago (Table 2). These sandy lacustrine sediments could also be a source for some of the recently recognized loess in southeastern Lower Michigan (Schaetzl et al., Reference Schaetzl, Luehmann, Peter, Connallon, Smidt, Liu, Kincare, Walikowiak, Thorlund and Holler2015).
Inland dune activity in the western Great Lakes region
Our OSL ages add to a growing number of OSL-dated dune studies that show a peak of eolian dune activity in the western Great Lakes centered at near the end of the Younger Dryas event at the Pleistocene-Holocene transition (Fig. 9). A review of OSL-dated inland dunes located around Lake Michigan (Fig. 9) demonstrates that eolian dune activity and stabilization also peaked slightly after the end of the Younger Dryas event in most of these areas (Figs. 10 and 11). These studies and our new data provide a total of 57 OSL age analyses whose mean is centered on the Pleistocene-Holocene transition (Rawling et al., Reference Rawling, Hanson, Young and Attig2008; Campbell et al., Reference Campbell, Fischer and Goble2011; Kilibarda and Blockland, Reference Kilibarda and Blockland2011; Arbogast et al., Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015). We assumed (as the original authors did) that all of our probability density distributions represented single events, except for the ages of Campbell et al. (Reference Campbell, Fischer and Goble2011), which both the authors and we assume record at least two dune-forming events.
(color online) Location of late Pleistocene to early Holocene dune fields in the western Great Lakes region. Arrows indicate the approximate reconstructed wind directions and age ranges in each study. Thick dashed line is the approximate terminus of the retreating Laurentide Ice Sheet at ~12.9 ka and during the main phase of Glacial Lake Algonquin, which is shown with the thin dotted line (after fig. 5 of Arbogast et al., Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015). (1) Ottawa County, Michigan, dune field (this study). (2) Roscoe dune field of north-central Lower Michigan (Arbogast et al., Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015). (3) Coastal spits cited by Krist and Schaetzl (Reference Krist and Schaetzl2001) as evidence for easterly winds along the front of the retreating Laurentide Ice Sheet. (4) Dune fields of northeastern Indiana and northwestern Ohio (Campbell et al., Reference Campbell, Fischer and Goble2011). (5) Dune fields of northwestern Indiana (Kilibarda and Blockland, Reference Kilibarda and Blockland2011). (6) Green River Lowland of northwestern Illinois (Miao et al., Reference Miao, Hanson, Wang and Young2010). (7) Dunes and elongated ice-walled lake plains used by Allred et al. (2014) to reconstruct paleowind directions at ~17,000 cal yr BP. (8) Central Sand Plain of Wisconsin (Rawling et al., Reference Rawling, Hanson, Young and Attig2008). (9) Early Holocene dunes in Upper Michigan (Loope et al., Reference Loope, Loope, Goble, Fisher, Jol and Seong2010).
Probability density and histogram plots for dune fields formed between ~14 and 10 ka (see Fig. 9 for site locations). The circles under the plots are individual sample means. The y-axis is number of samples in histograms, and the x-axis is ka before present. Ages correspond to approximate peaks in probability density function plots. The plots were constructed using DensityPlotter v. 7.1 (Vermeesch, Reference Vermeesch2012).
Comparison of dune field mean ages (black squares) to the oxygen isotope record of the North Greenland Ice Sheet Project (NGRIP) ice core. Drainage of Glacial Lake Chicago occurred at ~13.6 ka based on the existing radiocarbon chronology (Larson, Reference Larson2011). Large arrows show peaks of probability density plots determined from Figure 10. Peaks in dune optically stimulated luminescence ages occur during or shortly after the Younger Dryas event and the Preboreal event (PB). Three outlier samples (<4 ka) shown in Figure 9 were not included in the mean for data from Kilibarda and Blockland (Reference Kilibarda and Blockland2011). One late Holocene outlier (~0.79 ka) was not included in the mean and standard deviation for data of Campbell et al. (Reference Campbell, Fischer and Goble2011).
Rawling et al. (Reference Rawling, Hanson, Young and Attig2008) provided 24 OSL ages for eolian dune activity in the Central Sand Plain of Wisconsin, which formed after Glacial Lake Wisconsin drained at ~15,000 cal yr BP. These OSL ages range from 19.3±1.7 to 5.8±0.4 ka. The peak of the probability density distribution of their ages is ~11.5 ka, and the arithmetic mean and 1 standard deviation is 11.8±2.7 ka (Fig. 10). This peak correlates with the end of the Younger Dryas event (Fig. 11). Rawling et al. (Reference Rawling, Hanson, Young and Attig2008) proposed three different hypotheses to explain eolian activity and dune stabilization: (1) aridity caused by a climate event, (2) deflation of outwash in the Wisconsin River valley, and (3) melting of permafrost developed on the lake plain, which lowered water tables enabling deflation. They found the most attractive hypotheses to be deflation of outwash or melting of permafrost, which then lowered water tables and led to enhanced eolian deflation. This hypothesis is attractive because the peak of the ages occurs at the end of the Younger Dryas event, a time when the climate was changing from cool and dry to a warmer and wetter climate of the early Holocene. Dune activity during the Younger Dryas was then followed by dune stabilization once Holocene climate conditions were established after ~11.7 ka and surfaces became stabilized by vegetation cover.
Campbell et al. (Reference Campbell, Fischer and Goble2011) examined inland dunes in northeastern Indiana and northwestern Ohio (Fig. 9) and provided 10 OSL ages that range between 14.1±1.0 and 8.8±0.5 ka (excluding a single young age of 0.79±0.1 ka). These 10 OSL ages have two peaks in the probability density distribution, one at ~12.5 ka and another at ~9.0 ka (Fig. 10). They suggested that eolian activity on susceptible deflation surfaces was enhanced during the cooler and drier Younger Dryas event and the subsequent Preboreal oscillation and can be used to compliment pollen records of climate, which also suggest cooler and drier conditions at this time (Campbell et al., Reference Campbell, Fischer and Goble2011).
Inland dunes of the Fair Oaks dune field in northeastern Indiana (Fig. 9) yielded four OSL ages ranging from 12.5 to 11.2 ka (Kilibarda and Blockland, Reference Kilibarda and Blockland2011). These dunes also yielded three much younger OSL ages less than 4 ka that they interpreted as reflecting late Holocene reworking. Excluding the three younger ages, the probability density distribution shows a peak at ~11.5 ka and mean and standard deviation of 11.9±0.6 ka (Figs. 10 and 11). Kilibarda and Blockland (Reference Kilibarda and Blockland2011) argue that their observations and OSL ages indicate dune building began during the Bølling-Allerød event when easterly and northeasterly winds, attributable to anticyclonic circulation over the retreating ice sheet, formed transverse and barchan dune ridges. This dune-building event was then followed by reworking of the dunes during the Younger Dryas event by westerly winds that formed a great variety of parabolic dunes.
Most recently, Arbogast et al. (Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015) provide 10 OSL ages for eolian dune activity in the Rosco dune field of central Lower Michigan (Figs. 1B and 9). These OSL ages range from 13.0±1.2 to 9.7±0.8 ka. The peak of the probability density distribution is ~10.5 ka, with a mean and standard deviation of 11.1±1.0 ka (Fig. 10). This peak occurs slightly after the Preboreal oscillation (Fig. 11). The probability density distribution of all 57 OSL ages including our 6 new ages shows a peak occurring at ~11.5 ka slightly after the end of the Younger Dryas event during the Preboreal oscillation (Figs. 10 and 11).
Climate reconstruction based on pollen and permafrost evidence
Reconstructions of paleoenvironments and climate of Lower Michigan during the Bølling-Allerød and Younger Dryas events, based on plant macrofossils and pollen from inland lake sediment cores, indicate cool and dry conditions (Hupy and Yansa, Reference Hupy and Yansa2009). Black spruce (Picea mariana) and sedges were common in low areas because of wet soils attributable to melting buried glacier ice and permafrost, whereas open white spruce (Picea glauca) parklands favored the drier uplands (Hupy and Yansa, Reference Hupy and Yansa2009). Tundra plants and widespread fossil ice-wedge casts and ice-wedge polygons suggest that tundra vegetation and permafrost were present in eastern Wisconsin up to at least 13,000 cal yr BP (Maher and Mickelson, Reference Maher and Mickelson1996; Maher et al., Reference Maher, Miller, Baker, Curry and Mickelson1998, Clayton et al., Reference Clayton, Attig and Mickelson2001). Relict ice-wedge polygons found on the abandoned surface of Glacial Lake Saginaw in Lower Michigan also indicate that permafrost formed after lake drainage sometime during the Bølling-Allerød warming event and the subsequent Younger Dryas cooling (Lusch et al., Reference Lusch, Stanley, Schaetzl, Kendall, Van Dam, Nielsen and Blumer2009). Cool climate, terrestrial gastropods followed by boreal forest indicate ice-free conditions at the Two Creeks site in eastern Wisconsin and the Cheboygan bryophyte site in northern Lower Michigan during the Bølling-Allerød event (Larson, Reference Larson2011; Rech et al., Reference Rech, Nekola and Pigati2012). All of these observations suggest that Younger Dryas cooling and drying in an area already affected by permafrost provided a suitable environment for eolian deflation of the recently exposed nearshore sediments of Glacial Lake Chicago in the drier uplands of the study area.
Implications for paleolake level history in western Michigan
Figure 12 illustrates our reconstructions of paleolake levels in the study area (Table 1). Glacial Lake Chicago reached elevations of between ~202 and ~204 m amsl, sometime between ~17,000 and ~15,200 cal yr BP (Table 1 and Fig. 12A). It is notable that the areas covered by inland dunes in the study area were still covered by Glacial Lake Chicago until after the end of the Calumet Phase at ~13,600 cal yr BP (Fig. 12), and therefore, dunes could not have been formed before then. Our OSL ages are compatible with this conclusion because our oldest age is 13.3±1.1 ka and must have formed after drainage of Glacial Lake Chicago, inland of the shorelines of Glacial Lake Algonquin and postglacial Lake Chippewa (Table 1, Fig. 12C). The abandoned bed of Glacial Lake Chicago in the study area was exposed during the Glacial Lake Algonquin and Lake Chippewa levels and up until the present time. Inland dunes formed and stabilized during the Younger Dryas event and perhaps as late as the Preboreal event. During the early Holocene, dunes were stabilized by vegetation and crosscut by erosion of the Pigeon River and other rivers in the study area. The mid-Holocene Nipissing high stand was reached sometime after about 5500 cal yr BP (Baedke and Thompson, Reference Baedke and Thompson2000). This supports our interpretation that the inland dunes are older than the Nipissing high because terraces in the Pigeon River valley both truncate dunes and do not have dunes on terrace surfaces (Fig. 12C). Most of the large, relatively young coastal dunes lie on the surface flooded by Lake Nipissing and have constricted the Pigeon River by encroachment of dune sand at the river mouth.
(color online) Time-series reconstructions of lake levels during the late Pleistocene and Holocene mapped using a digital elevation model and estimates of lake levels from landforms and sediments in the county. (A) Glenwood I and II levels of Glacial Lake Chicago (~203 m amsl). (B) Calumet level of Glacial Lake Chicago (~195 m amsl). (C) Postglacial Lake Nipissing at its maximum level in Ottawa County (~186 m amsl) and the location of inland parabolic dune fields outlined in fine black lines (i). (D) Modern lake level of Lake Michigan with areas of inland parabolic dune fields outlined with black lines (i). The lake bed of Glacial lake Chicago would have been exposed after the fall from the Calumet level after ~13.6 ka (panel B).
Paleowinds in the western Great Lakes region
Studies in the western Great Lakes region have provided new information on paleowinds reconstructed from OSL-dated inland dunes during the Pleistocene-Holocene transition (Fig. 9). Easterly winds are inferred from spits that developed in glacial Lake Algonquin between ~13.6 and 11 ka (Krist and Schaetzl, Reference Krist and Schaetzl2001; Vader et al., Reference Vader, Zeman, Schaetzl, Anderson, Walquist, Freiberger, Emmendorfer and Wang2012) and from dunes in northwestern Indiana (Kilibarda and Blockland, Reference Kilibarda and Blockland2011). These studies hypothesize that easterly winds were the result of anticyclonic circulation above the retreating Laurentide Ice Sheet as predicted in atmospheric models of late Pleistocene circulation (Kutzbach and Guetter, Reference Kutzbach and Guetter1986; Broccoli and Manabe, Reference Broccoli and Manabe1987; COHMAP Members, 1988).
All of the recently OSL-dated inland dune fields cited in the previous section indicate northwesterly and westerly winds during the late part of the Bølling-Allerød, Younger Dryas event, and the Preboreal oscillation (Fig. 9). Undated inland dunes in the Saginaw dune field of Lower Michigan (Fig. 9) also indicate winds from the northwest and west after about ~15,000 cal yr BP (Arbogast et al., Reference Arbogast, Scull, Schaetzl, Harrison, Jameson and Crozier1997; Arbogast and Jameson, Reference Arbogast and Jameson1998). The northwesterly and westerly directions confirm previous interpretations that the anticyclonic circulation must have been limited in its effects after the late part of the Bølling-Allerød event and during the Younger Dryas event (Arbogast et al., Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015; Kilibarda and Blockland, Reference Kilibarda and Blockland2011). This was also the interpretation of Rawling et al. (Reference Rawling, Hanson, Young and Attig2008) for the inland dunes that formed in the Central Sand Plain of Wisconsin as no evidence was found there for easterly winds even though some of these dunes were older than the Bølling-Allerød. Arbogast et al. (Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015) proposed that there must have been a very steep energy gradient to the winds because easterly wind directions were apparently occurring less than 150 km from northwesterly winds (Fig. 5 of Arbogast et al., Reference Arbogast, Luehmann, Miller, Wernette, Adams, Waha and O’Neil2015). Our observations provide no evidence for easterly anticyclonic winds nor evidence against a steep energy gradient hypothesis. In summary, inland dunes in this study, and three of four sites with OSL ages reviewed previously, provide no support for anticyclonic easterly and northeasterly winds during the latest part of the Bølling-Allerød event and the subsequent Younger Dryas event.
CONCLUSIONS
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1. Inland dunes are common on the abandoned bed of Glacial Lake Chicago in Ottawa County and surrounding coastal counties in western Lower Michigan. Inland dunes have parabolic forms and are modified by blowouts and human disturbance.
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2. Six new OSL ages indicate that inland dunes formed and stabilized between 13.3±1.1 and 11.6±0.9 ka (2-sigma uncertainty). Soils developed on the inland dunes, radiocarbon ages on buried organics in the Pigeon River valley, and stratigraphic and landform relationships all corroborate our OSL ages.
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3. The inland dunes in the study area formed and stabilized after drainage of Glacial Lake Chicago at ~13,600 cal yr BP during the late Bølling-Allerød, Younger Dryas, and Preboreal events.
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4. The source of inland dune sand was the gravelly, medium to fine nearshore sand on the abandoned bed of Glacial Lake Chicago. Sand was deflated by northwesterly and westerly winds, before vegetation was able to completely stabilize sandy nearshore lake sediments.
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5. Four other OSL-dated dune fields in the western Great Lakes region also show that eolian activity driven by northwesterly and westerly winds was a widespread phenomenon during the Pleistocene-Holocene transition. This supports a hypothesis that changing climatic conditions at the Pleistocene-Holocene transition and the availability of recently deglaciated surfaces provided an ideal environment for eolian activity.
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6. Evidence of northwesterly and westerly winds at all of these sites supports previous interpretations of the limited effect of an anticyclone developed over the retreating Laurentide Ice Sheet.
Acknowledgements
Funding to undergraduate student Sara Thurkettle was provided by a Norman and Helen Gibson Summer Scholarship for summer of 2015 (Grand Valley State University). We thank lead park naturalist Kristen Hintz and Ottawa County Parks for access to sites in Pigeon Creek and Hemlock County Parks. Tom Valachovics, Andrew Alder, and Alexander Rarick helped with field sampling. Nick Colaianne shared grain-size data from Kirk Park. Grand Valley State University undergraduates Spencer Brower, Reece Elling, Natalie Renkes, Mike Moon, and students in P.C.’s winter 2016 geophysics class helped collect and process the GPR data from Pigeon Creek Park. J. Teller and an anonymous reviewer provided useful comments to help focus and improve the manuscript.
Supplementary material
To view supplementary material for this article, please visit https://doi.org/10.1017/qua.2016.13
Open access
