Glacial stratigraphy of Stough Creek Basin, Wind River Range, Wyoming

Geomorphology 42 (2002) 59 – 83 www.elsevier.com/locate/geomorph

Glacial stratigraphy of Stough Creek Basin, Wind River Range, Wyoming Dennis E. Dahms * Department of Geography, 127 Sabin Hall, University of Northern Iowa, Cedar Falls, IA, 50614-0406, USA Received 17 March 2000; received in revised form 29 March 2001; accepted 30 March 2001

Abstract Multiparameter relative-age (RA) techniques identify four post-Pinedale morphostratigraphic units in each of three cirque valleys tributary to Stough Creek Basin, Wind River Range, WY. Soil development, lichenometry, boulder weathering characteristics, and the geomorphic relations among morphostratigraphic units indicate glacial deposits here correspond to the sequence previously described in the Temple Lake valley [Arct. Alp. Res. 6 (1974) 301]. Cirque deposits in Stough Creek Basin correspond to the Temple Lake, Alice Lake, Black Joe, and Gannett Peak alloformations [GSA Abs. Prog. 32 (2000) A-16]. 10 Be ages from moraine boulders and polished-striated bedrock [Assoc. Am. Geogr. Annu. Mtg. Abs. (2000) 155] support recent numeric age estimates from Temple Lake and Titcomb Basin that indicate the Temple Lake Alloformation corresponds to the Younger Dryas climate episode [Geogr. Phys. Quat. 41 (1987) 397; Geology 23 (1995) 877; Science 268 (1995) 1329; GSA Abs. Prog. 31 (1999) A-56]. Soils described from Pinedale recessional deposits here represent the first systematic description of Pinedale alpine deposits in the WRR. D 2002 Elsevier Science B.V. All rights reserved. Keywords: Wind River Range; Relative age data; Glacial stratigraphy; Younger Dryas; Neoglacial

1. Introduction Systematic mapping and correlation of late Pleistocene and Holocene alpine glacial successions have implications for interpretations of Quaternary climate change outside of any particular mountain range. Such work has implications for both local and regional clarification of glacial history and associated paleoclimatic reconstruction. Maps of downvalley extent(s) of glacial deposits often are used to indicate paleoclimatic fluctuations based on the assumption that ice

*

Tel.: +1-319-273-6845; fax: +1-319-273-7103. E-mail address: [email protected] (D.E. Dahms).

volume can be inferred from glacial extent (Gosse et al., 1995a). Interpretations of the post-Pinedale glacial succession for the Wind River Range, WY (WRR) are based on the cumulative relative and numeric age data gathered by numerous workers from a number of cirque valleys (Holmes and Moss, 1955; Currey, 1974; Mears, 1974; Miller and Birkeland, 1974; Mahaney, 1978, 1984a,b; Zielinski and Davis, 1987; Gosse et al., 1995a,b, 1999). The main points of contention have been the number and timing of post-Pinedale glacial events recorded in the valleys. The Temple Lake valley and Titcomb Basin are the only localities from which published descriptions exist for deposits corresponding to all post-Pinedale

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glacial events in the WRR [Temple Lake– Early Neoglacial (Indian Basin) – Audubon equivalent – Gannett Peak; Miller and Birkeland, 1974; Mahaney, 1978, 1984b]. Previous relative age (RA) studies of glacial deposits in the US intermountain west and Rocky Mountains show that the best results are produced using combinations of methods (e.g., soil development, lichenometry, boulder weathering: Birkeland, 1973; Burke

and Birkeland, 1979). My purpose here is, likewise, to use a number of methods to assign relative ages to the glacial deposits in Stough Creek Basin. Methods used for this study include unit characteristics (morphology, and position relative to other units), lichen sizes, and soil development characteristics. I first use RA data to identify five morphostratigraphic units in each of the three cirques (Helen Lake, Bigfoot Lake, Ice Lake). I then assign the morphostratigraphic units to corre-

Fig. 1. Digital image of the Wind River Range shows the location of Stough Creek Basin in relation to regional landmarks and localities from which post-Pleistocene stratigraphic units previously have been described.

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Fig. 2. Overview (A) of Stough Creek Basin and detailed views of Helen Lake (B) and Bigfoot Lake (C) cirques. (A) Southern half of Stough Creek Basin, looking SW from soil RFP-2. The classic ‘‘biscuit-board’’ topography of the southern Wind River Range is easily seen here. The post-Pinedale units described in Helen and Bigfoot Lake cirques are shown in (B) and (C); (B) from north; (C) from NE.

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sponding allostratigraphic units (Birkeland and Miller, 1989; Birkeland, personal communication, 1998; Dahms and Birkeland, 2000) with the help of minimum-limiting 10Be and 26Al numeric ages derived from moraine boulders and polished/striated bedrock (Dahms et al., 2000). Data presented here support the interpretations that (i) deposits corresponding to the Temple Lake alloformation (Dahms and Birkeland, 2000) were deposited near the time of the Younger Dryas event (Miller and Birkeland, 1974; Zielinski and Davis, 1987; Gosse et al., 1995a; Davis et al., 1998), and that (ii) deposits of three Neoglacial (Porter and Denton, 1967) ice advances are recorded in the cirque valleys of the WRR (Miller and Birkeland, 1974; Birkeland, personal communication, 1998; Dahms and Birkeland, 2000).

2. Study area The Wind River Range is located in the middle Rocky Mountains of west central Wyoming (Fig. 1). The range is approximately 225 km long and 48 km wide, and its crest forms nearly 200 km of the US western continental divide. Stough Creek Basin is located in the southeastern part of the WRR, 30 km SW of Lander, WY and 14 km SE of the Temple Lake valley. The southern and western boundaries of the basin follow the continental divide roughly between Atlantic Peak and Wind River Peak, 12 km to the NW. Three main cirques are tributary to Stough Creek Basin: Helen Lake, Bigfoot Lake, and Ice Lake cirques (Figs. 2 and 3). Elevations of the permanent snowfields are 3444 m (11,300 ft) in Helen Lake cirque, 3414 m (11,200 ft) in Bigfoot Lake cirque,

Fig. 3. Distribution of mapped allostratigraphic units in Stough Creek Basin, including soil sampling sites and the localities for ages noted in the text (from Dahms et al., 2000).

10

Be and 26Al

D.E. Dahms / Geomorphology 42 (2002) 59–83

and 3383 m (11,100 ft) in Ice Lake cirque. Elevations of cirque riegels are 3383 m (11,100 ft) in Helen Lake cirque and 3322 m (10,900 ft) in Ice Lake and Bigfoot Lake cirques. The riegels dam the largest lake in each cirque. The dominant bedrock lithology here is Archean granite and granodiorite associated with the Louis Lake batholith (Love and Christiansen, 1985). Local climate data was obtained from a 122-day sampling period in the summer of 1992 (June – October). Two microclimate stations located above Stough Creek Basin on Roaring Fork Mountain at 3383 m (11,096 ft) recorded average summer air temperatures of 5– 9 °C within 10 cm of ground level. Daily maxima ranged from 10 – 16 °C and daily minimums averaged 0– 3 °C (R.W. Scott, personal communication, 1999). Wet deposition of 90 – 134 cm/year was reported from 1986 to 1989 from bulk snow and water collectors located at Black Joe Lake, ca. 15 km NW of Stough Creek Basin (Galbraith et al., 1991). Mean air temperature was
6.9 °C on Upper Fremont Glacier in the northern part of the WRR between July 11, 1990 and July 10, 1991 (Naftz and Miller, 1992).

3. Relative dating methods Four methods are used to differentiate the glacial deposits of the basin, following the reasoning articulated by Birkeland (1973) for Mt. Sopris, CO, that ‘‘no single relative age-dating method is sufficiently sensitive to date all the deposits.’’ I combined geomorphic and stratigraphic relations among the morphostratigraphic units in each cirque basin with detailed soil development and lichen data and a limited amount of boulder weathering data. Miller and Birkeland (1974) and Mahaney (1978, 1984b) used similar methods in the WRR in Temple Lake valley, Titcomb, and Indian Basins, respectively. 3.1. Morphology of morphostratigraphic units Unit boundaries were delineated by walking field contacts and noting these on USGS NAPP aerial photographs and on the Sweetwater Gap and Cony Mountain, WY, 7.5-ft USGS topographic quadrangle maps. Contacts between adjacent units in each cirque

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were tentatively identified on the basis of morainal topography, the amount of turf formed on each unit, boulder weathering estimates, and percent lichen cover on boulders. 3.2. Lichenometry Lichen size, percent cover of all lichens on boulder surfaces, and proportions of lichen species are demonstrated to change over time in alpine environments of the Rocky Mountains (Beschel, 1957, 1961; Benedict, 1967, 1973, 1981, 1985, 1996; Birkeland, 1973; Matthews 1973, 1974, 1975, 1977; Miller and Birkeland, 1974; Locke et al., 1979; Birkeland and Miller, 1989). Lichens in the Rocky Mountain region reportedly colonize, grow to their maximum size(s), then fragment into smaller individuals and colonies over 4 –5 ka (Benedict, 1967). Lichenometry is integrated in this study with soil development data in order to (i) identify and separate morphostratigraphic units and (ii) refine the RA age estimates. I measured only the yellow-green lichen commonly known as Rhizocarpon geographicum as it is a common lichen found on the moraine boulders in the Rocky Mountains and is used extensively in previous age and growth-rate studies (Benedict, 1967; Birkeland, 1973; Miller and Birkeland, 1974; Birkeland and Miller, 1989; Birkeland, personal communication, 1998). Field identification is difficult and laboratory study is usually necessary for correct identification (Locke et al., 1979; Innes, 1985). For this reason, Rodbell (1992) suggested the term Rhizocarpon subspecies Geographicum. I use the term R. geographicum in the broad sense, for the yellowgreen Rhizocarpon species (here termed R. geographicum, s.l. (sensu lato)). I measured to the nearest millimeter a minimum of 100 lichens on each unit in each cirque. Only lichens with circular or slightly elongate outlines were measured; of these, I measured only the smallest diameter of the two largest lichens on each boulder to avoid over estimating the size of lessthan-circular lichens. Lichens were measured only on boulders 1 m diameter to avoid boulders that might have moved since deposition. No lichens were measured below 20 cm from ground level in order to minimize microclimatic effects. The largest lichens generally were found on NW to NE sides of boulders

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(Birkeland noted a similar situation on Mt. Sopris, CO). 3.3. Soil development Soil development is used routinely in RA studies of alpine glacial deposits in the western US (Richmond, 1957, 1962; Birkeland, 1973, 1999; Burke and Birkeland, 1979; Birkeland et al., 1991a,b; Berry, 1994), including alpine deposits of the WRR (Miller and Birkeland, 1974; Mahaney, 1978, 1984a,b; Mahaney et al., 1984a,b; Swanson, 1985; Hall and Shroba 1993, 1995). Miller and Birkeland (1974) reported that the most useful time-dependent soil parameters on post-Pinedale deposits in the WRR are the intensity and depth of oxidation. On Pleistocene deposits of the WRR, the increase in clay content of B horizons and the degree of clay – mineral alteration also are useful (Shroba and Birkeland, 1983). For this study, I use four parameters to estimate soil age: B horizon development, profile depths (depth to Cox-C boundary), pedogenic silt and clay, and the Profile Development Index (PDI) of Harden (1982). Soils were described and sampled from hand-dug pits using standard methods and horizon nomenclature (Birkeland et al., 1991a; Soil Survey Staff, 1994, 1999; Birkeland, 1999). I distinguish between Bw and Cox horizons by Munsell color; the Bw being 10YR hue and the Cox being 2.5Y hue. I use the designation Btj (National Soil Survey Committee of Canada, 1974) for horizons that contain translocated clay in insufficient amounts to meet the requirements for an argillic horizon (Soil Survey Staff, 1999). Laboratory analyses used standard techniques modified from Klute (1986) and Singer and Janitzky (1986). Particle-size distribution was determined by the sieve and pipette method. Prior to PSD analysis, organic carbon was removed from the samples with 30% H2O2. Bulk density was determined by the paraffin-clod method for gravel-free peds using a gravel density of 2.6 g/cm3. Bulk density values were obtained from the average of at least two peds where the soil matrix was sufficiently cohesive. Where cohesive peds were not available, bulk density estimates were obtained by averaging values from similar horizons in Stough Creek Basin or from

other WRR locales (Dahms, 1991). Particle-size distribution is reported as weight percent (USDA scale). Percentages of silt and clay also were calculated as g/cm2 in order to identify actual additions/losses in each horizon, following McCalpin and Berry (1996): %  bulk density  horizon thickness (1
% > 2 mm=100Þ: To further describe actual amounts of silt and clay present in each profile, I calculated amounts of silt and clay produced by pedogenesis in whole profiles (termed pedogenic silt or clay) by the following method (McCalpin and Berry, 1996): g=cm2 =profile ¼ Rf½ð%clayh  BDh  Th Þ
ð%claypm  BDpm  Th Þ (1
vol:%Gh Þ; where h is horizon value, BD is gravel-free bulk density, T is horizon thickness, pm is parent material value, and G is gravel (Taylor, 1986); vol.% Gh= (wt.% Gh/dG)/[(wt.% Gh/dGh)+{(1
wt.% Gh)/BDh}], where d is density (Soil Conservation Service, 1972). Note that much of the clay in young soils here is thought to be derived from eolian dust (Birkeland et al., 1991b; Dahms, 1993; Dahms and Rawlins, 1996) and that relatively little clay is due to in situ weathering. I consider clay derived from eolian dust as pedogenic in nature, since dust-accumulated fines are generally regarded to have a considerable influence on soil genesis (e.g., Muhs, 1983; McFadden and Weldon, 1987; McFadden, 1988; Reheis et al., 1989, 1995; Harden et al., 1991; McCalpin and Berry, 1996). Silt and clay contents of C horizons were used to estimate parent material values from which to calculate amounts of pedogenic silt and clay. I convert soil field properties to numerical values using the PDI of Harden (1982) as another method by which soil development among stratigraphic units might be compared (see discussion of method in Birkeland et al., 1991a). Properties quantified for the index here include moist and dry rubification, moist and dry melanization, total texture, moist and dry consistence, and structure.

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1). Less than 10% of boulders are weathered or show oxidation and minimal pitting was noted.

4. Relative age data 4.1. Morphostratigraphy of deposits Helen Lake and Bigfoot Lake cirques contain deposits that represent five glacial events. I interpret these to represent one Pinedale and four post-Pinedale events (Figs. 2A,B and 3). Ice Lake cirque contains deposits representing the four post-Pinedale events. The deposits here initially are described as, from youngest to oldest, morphostratigraphic units 1– 5. 4.1.1. Morphostratigraphic unit 1 Unit 1 terminates 0.5 km downvalley of the cirque headwalls in Helen Lake and Bigfoot Lake cirques, at 3393 m (Fig. 3). Unit 1 consists of fresh till with large boulders (2– 5 m diameter) with little fine matrix between clasts except at a few sites where sandy material is concentrated. The deposit is near its angle of repose and boulders often shift unsteadily underfoot. Boulders are angular, unweathered, and unpitted and their surfaces mostly are fresh gray although some are slightly oxidized (Table 1). Permanent snowfields connect unit 1 with the headwalls in Helen Lake and Bigfoot Lake cirques. 4.1.2. Morphostratigraphic unit 2 Unit 2 in Helen Lake cirque lies adjacent to the SE boundary of unit 1 (Fig. 3). In Bigfoot Lake, unit 2 encloses unit 1 in a rough semi-circle. Unit 2 in Ice Lake cirque has no interstitial fines between boulders and so is more likely a protalus deposit than till. Boulders in all cirques are similar in size to those of unit 1 with corners that are not quite as angular (Table

4.1.3. Morphostratigraphic unit 3 Unit 3 lies just beyond and below the unit 2 termini in all cirques (Fig. 3). The units in Helen Lake and Bigfoot Lake cirques have full tundra cover. Unit 3 is similar to unit 2 in Ice Lake, however, and is distinguishable only by lichenometry. Weathering pit depths were not measured systematically, but boulders on unit 3 show some shallow pitting (Table 1). Boulders have more oxidation and 30% rounded corners. The characteristics are not as pronounced in Ice Lake cirque. 4.1.4. Morphostratigraphic unit 4 Unit 4 lies just downvalley and beyond unit 3 in all cirques (Fig. 3). Unit 4 at Bigfoot Lake and Ice Lake has full tundra cover, while in Helen Lake cirque the unit has less tundra cover than units 3 or 5. Nearly all boulders are weathered and pits occur frequently (Table 1). Prominent pits often are found on vertical faces of boulders. 4.1.5. Morphostratigraphic unit 5U Unit 5U termini are located significantly farther downvalley than unit 4 (Fig. 3). The termini of unit 5U are located below each cirque riegel, which, in turn dams the largest lake in both Helen Lake and Bigfoot Lake cirques. Unit 5U is not identified in Ice Lake cirque. The alpine turf cover on unit 5U is the most complete of any unit mapped in this study. Boulder weathering characteristics are most developed on this unit (Table 1).

Table 1 Lichen and weathering data Unit

Percent cover

Minimum diameters (mm)

Mean five largest thalli (mm)

Boulders (%) Pitted

Weathered

1 2 3 4 5U

0–5 5 – 40 50 – 85 85 50

10 – 16 10 – 57 10 – 88 19 – 67 30 – 67

13.2 54 79.8 64.8 64.2

0 Few to none <25 Prominent on vertical faces, 50 75

0 <10

30 All rounded and oxidized All rounded and oxidized

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4.1.6. Morphostratigraphic unit 5L Deposits below the cirque riegels are mapped as unit 5L and appear to represent the upper margins of latest Pleistocene ice and recessional positions of the ice (Fig. 3). Stagnant ice deposits consist of boulders and gravel supported by material that generally contains more sand than units 3, 4, and 5U (Table 3). Numerous erratics are perched on polished and striated rouche moutone´e. Crystals of quartz and feldspar stand in relatively high relief on many boulders, and single crystals can be broken off easily by hand. 4.2. Lichen data Unit 1 exhibits a few, small lichens on boulders and the lichens appear only singly and not in colonies. Boulders of unit 2 exhibit 5 –40% lichen cover and roughly equal numbers of green and brown/black lichens. Lecanora thompsonii (brown/black) are especially large and prominent. The maximum thallus diameter and the mean of the five largest Rhizocarpon thalli are noticeably larger than those of unit 1 (Table 1). Unit 3 boulders show more complete lichen cover than those of units 1– 2. Brown/black varieties are more abundant than green, so that only 50 –60% of boulders >1.0 m diameter exhibit Rhizocarpon. Rhizocarpon tends to colonize the NW or W faces of boulders and the lower 0.5 m of the boulders in Helen Lake and Bigfoot Lake cirques. Rhizocarpon occurs more randomly on the boulders in Ice Lake cirque. The largest mean and maximum Rhizocarpon thalli diameters of the study were recorded on this unit. Unit 4 exhibits the most complete lichen cover, so that >60% of boulders 1.0 m diameter have Rhizocarpon. Rhizocarpon again colonize the NW or W face of the boulders, and most lichens are found on the lower 0.5 m of the boulders. Mean and maximum Rhizocarpon thalli diameters are smaller here than on unit 3 (Table 1). Boulders of unit 5U exhibit less complete lichen cover, so that less than 30% of the boulders <2 m in diameter have Rhizocarpon. Lichens appear to be mostly Lecanora and Lecidea species. Mean and maximum Rhizocarpon thalli diameters are similar to those of unit 4. Lichen data were not collected on unit 5L.

4.3. Soil development Soils on all morphostratigraphic units above treeline (units 1– 5U) developed in stony coarse sandy till (Fig. 3; Table 3) overlain by various thicknesses of mixed loess (Shroba and Birkeland, 1983; Dahms, 1993). Few interstitial fines are present on units 1 and 2, so that only one profile on unit 1 (BFL9) and only two profiles on unit 2 (BFL8, SCB12) could be described (Tables 2 and 3). Soils on units 1 and 2 have Cox/C or A/Cox/C horizons with 10YR hues in A horizons and 2.5Y hues in Cox horizons. C horizons are 5Y hues. Profile depths are minimal (Table 2; Fig. 4). So few soils have developed on these units that these profiles may not be representative of similar units described elsewhere in the WRR (Birkeland, personal communication, 1998). Profile depths progressively increase from unit 3 to unit 5L (Fig. 4). Soils on unit 3 have A/Bw/Cox/C or A/Bt/Cox/C horizons with 10YR hues above Cox horizons (Table 2). Unit 3 diagnostic B horizons are both cambic and argillic. Depths to the base of B horizons vary from 15 to 20 cm and B horizon thickness varies from 8 to 12 cm. Soils on unit 4 all have A/Bt/Cox/C profiles. B horizons all are argillic (Table 3). Depths to the base of B horizons vary from 13 to 55 cm and B horizon thickness varies from 8 to 40 cm. Profiles on unit 5U all have A/Bt/Cox/C horizons, except SCB3 (Table 2). All B horizons are argillic except that of SCB3. Depth to the base of B horizons varies from 27 to 60 cm and thicknesses of B horizons from 19 to 42 cm. Except for RFP1, RFP2, WL1, and SCB10, soil profiles on unit 5L developed under mature subalpine forest. RFP1 and RFP2 are located above treeline on deposits that I interpret as a kame terrace and a lateral moraine, respectively (Fig. 3). SCB10 is located on what may be a lateral moraine remnant in Helen Lake cirque. WL1 is at treeline near a thick stand of krummholz. The forest profiles have weak spodic characteristics with E and/or Bs horizons (Table 2). The profiles above treeline contain Bw or Bt horizons (though SCB10 has a weakly expressed E horizon). Depth to the base of B horizons varies from 29 to 80 cm. Thickness of

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Table 2 Field descriptions for soils: Stough Creek Basin Munsell Color Profile

Horizon

Depth (cm)

Moist

Dry

Texturea

Consistenceb

Structurec

Morphostratigraphic Unit 1 BFL9 Cox Cu

0–5 5 – 25

2.5Y3/2 5Y4/1

2.5Y5/2 5Y5/2

LS LS

so-po/lo/lo so-po/lo/lo

sg sg

Morphostratigraphic Unit 2 BFL8 Cox Cu SCB12 A Cox 2Cu

0–5 5 – 25 0–2 2 – 10 10 – 30+

2.5Y3/2 5Y4/1 2.5Y3/2 5Y4/1 5Y4/1

2.5Y5/2 5Y5/2 2.5Y5/2 5Y5/2 5Y5/2

LS LS LS LS S

so-po/lo/lo so-po/lo/lo so-po/lo/lo so-po/lo/lo so-po/lo/lo

sg sg sg sg sg

Morphostratigraphic Unit 3 BFL6 A 2Bt 2Cox1 2Cox2 BFL7 A 2Bw 2Cox1 2Cox2 SCB6 A Bt 2Cox1 2Cox2 SCB7 A Bw 2Cox1 2Cox2

0 – 10 10 – 20 20 – 28 28 – 45+ 0–7 7 – 15 15 – 30 30 – 45+ 0–5 5 – 17 17 – 30 30 – 50+ 0–5 5 – 15 15 – 25 25 – 50+

10YR3/2 10YR4/3 2.5Y4/3 2.5Y4/4 10YR3/2 10YR4/3 2.5Y4/3 2.5Y4/4 10YR2/2 10YR3/4 2.5Y4/2 2.5Y4/2 10YR3/2 10YR3/4 10YR4.5/3 2.5Y4/2

10YR5/2 10YR5/3 2.5Y5/3 2.5Y6/2 10YR5/2 10YR5/3 2.5Y5/3 2.5Y6/2 10YR3/1 10YR3/2 10YR6/2 2.5Y6/2 10YR4/2 10YR5/2 2.5Y6/3 2.5Y6/2

SL SL SL SL SL SL SL SL L L SL SL SL SL LS LS

ss-po/lo/lo ss/po/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo so-po/vfr/so so-po/vfr/so so-po/lo/lo so-po/lo/lo ss-ps/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo so-po/vfr/so so-po/lo/lo so-po/lo/lo

1-f-gr 0.5-m-sbk sg sg 1-f-gr 0.5-f-sbk 0.5-f-sbk sg 1-vf-gr 0.5-f-gr sg sg 1-f-gr 0.5-f-gr sg sg

Morphostratigraphic Unit 4 BFL4 OA Bt 2Cox1 2Cox2 BFL5 A 2Bt 2Cox1 2Cox2 SCB8 A Bt 2Cox1 2Cox2 SCB9 A 2Bt 2Cox1 2Cox2 IL1 A 2Bt 2BC 2Cox

0–5 5 – 13 13 – 37 37 – 63+ 0–9 9 – 22 22 – 55 55 – 75+ 0–7 7 – 15 15 – 39 39 – 50+ 0–5 5 – 11 11 – 35 35 – 50+ 0 – 15 15 – 35 35 – 55 55+

10YR3/2 10YR4/3 2.5YY4/4 2.5Y4/4 10YR3/2 10YR4/3 2.5Y4/4 2.5Y4/2 10YR3/2 10YR3/4 10YR4/4 2.5Y4/3 10YR3/2 10YR3/4 10YR4/4 2.5Y4/2 10YR3/2 10YR4/4 10YR4/4 2.5Y5/4

10YR5/2 10YR5/3 2.5Y6/4 2.5Y6/2 10YR4/2 10YR5/4 2.5Y6/4 2.6Y7/2 10YR4/2 20YR4/3 2.5Y5/4 2.5Y6/3 10YR4/2 10YR4/3 2.5Y6/4 2.5Y6/2 10YR4/2 10YR5/4 10YR6/4 2.5Y7/3

SL SL SL SL SL SL SL LS L SL LS LS SL SL SL LS L SL SL SL

so-po/lo/lo ss-ps/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo ss-ps/vfr/so so-po/vfr/so so-po/lo/lo so-po/lo/lo ss-ps/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo ss-ps/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo ss-ps/vfr/so so-po/lo/lo so-po/lo/lo

1-f-gr 1-f-sbk sg sg 1-f-gr 0.5-f-sbk 0.5-f/m-sbk/gr sg 1-f-gr 1-m-gr sg sg 0.5-f-sbk 0.5-m-sbk 0.5-f-sbk sg 0.5-f-sbk 1-f-sbk 0.5-f-sbk sg

(continued on next page)

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Table 2 (continued) Munsell Color Moist

Dry

Texturea

Consistenceb

Structurec

Morphostratigraphic Unit 5U BFL1 A 0–8 Bt 8 – 18 2BC 18 – 27 2Cox1 27 – 65 2Cox2 65 – 90+ BFL2 A 0–5 AB 5 – 18 Bt 18 – 60 2Cox1 60 – 80 3Cox2 80+ BFL3 A 0 – 12 AB 12 – 23 Bt 23 – 60 Cox1 60 – 72 2Cox2 72+ SCB2 A 0–9 Bt 9 – 22 BC 22 – 33 2Cox 33 – 60+ SCB3 A 0 – 10 AB 10 – 26 2Bw 26 – 48 2Cox 48 – 65 2Cu 65 – 80+ SCB4 A 0–7 Bt 7 – 20 BC 20 – 43 Cox 43 – 55 2Cu 55 – 65+ SCB5 A 0 – 10 Bt 10 – 25 2BC 25 – 52 2Cox 52 – 62 2Cu 62+ SCB11 A 0–9 Bt 9 – 20 2BC 20 – 30 2Cox1 30 – 45 2Cox2 45 – 55+

10YR2/2 7.5YR3/2 2.5YR4/4 2.5YR4/4 2.5YR4/4 10YR2/2 7.5YR3/2 10YR4/4 2.5Y4/4 2.5Y4/4 10YR2/2 7.5YR3/2 10YR4/4 2.5Y4/4 2.5Y4/4 10YR3/2 10YR4/3 10YR3/3 2.5Y4/4 10YR3/1 10YR3/2 10YR3-4/3 2.5Y4/3 5Y4/2 10YR3/1 10YR4/3 10YR4/4 2.5Y4/4 5Y4/2 10YR3/1 10YR3/3 10YR5/4 2.5Y4/4 5Y4/2 10YR3/2 7.5YR3/4 10YR3/4 10YR4/4 2.5Y4/4

10YR3/2 7.5YR4/3 2.5YR7/4 2.5YR7/4 2.5YR6/4 10YR3/2 7.5YR4/3 10YR6/4 2.5Y6/4 2.5Y6/4 10YR4/2 7.5YR4/3 10YR6/4 2.5Y6/4 2.5Y6/4 10YR3/2 10YR4/4 10YR5/4 2.5Y6/4 10YR3/2 10YR4/3 10YR5/3 2.5Y6/3 5Y6/3 10YR3/1 10YR4/3 10YR5/4 2.5Y6/4 5Y6/3 10YR3/2 10YR4/2 10YR5/4 2.5Y6/3 5Y6/2 10YR3/2 10YR4/3 10YR5/4 2.5Y5/4 2.5Y6/3

SL SL LS SL LS SL SL SL SL LS SL SL SL SL LS SCL SL SL LS SCL SL LS L LS SCL SL SL L LS SL SL LS SL LS L L LS LS LS

so-po/lo/lo ss-ps/fr/so so-po/fr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo ss-po/fr/so ss-ps/vfr/so so-po/lo/lo so-po/lo/lo so-po/vfr/so ss-po/fr/so ss-ps/fr/so so-po/lo/lo so-po/lo/lo so-po/vfr/so ss-ps/vfr/so so-po/lo/lo so-po/lo/lo ss-po/vfr/so so-po/vfr/so so-po/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo ss-ps/vfr/so so-po/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo ss-ps/vfr/so ss-ps/vfr/so so-po/lo/lo so-po/lo/lo so-po/lo/lo ss-ps/vfr/so so-po/vfr/so so-po/lo/lo so-po/lo/lo

1-vf-gr 1-f-sbk 0.5-f-sbk sg sg 1-vf-gr 1-f-sbk 1-m-sbk 0.5-f-sbk sg 1-f-gr 0.5-f-sbk/gr 1-f-sbk/gr 0.5-f-sbk sg 1-f-gr 0.5-m-sbk 0.5-f-gr 0.5-f-gr 1-f-gr 1-f-sbk 1-m-sbk sg sg 1-f-gr 0.5-f-sbk/gr 0.5-f-sbk/gr sg sg 1-f-gr 1-m-sbk 0.5-f-sbk sg sg 1-vf-gr 1-m-sbk 1-f-gr sg sg

Morphostratigraphic Unit 5L SCB1 A E 2Bs1 2Bs2 2Cox1 2Cox2 SCB10 A Ej Bw 2ABb

10YR2/1 10YR4/4 7.5YR4/8 10YR4/7 2.5Y5/4 2.5Y5/2 10YR3/1 10YR3/3 7.5YR3/2 10YR2/2

10YR4/2 10YR5/3 10YR5/6 10YR6/6 2.5Y7/4 2.5Y7/2 10YR3/2 10YR4/3 10YR3/3 10YR4/2

SL L SL SL SL SL SiCL SiL CL SCL

ss-ps/vfr/so so-po/vfr/so ss-ps/fr/so ss-ps/vfr/so so-po/vfr/so so-po/lo/lo ss-ps/vfr/so ss-ps/vfr/so ss-ps/fr/so ss-po/vfr/so

1-f-gr 1-f-gr 1-m-sbk 0.5-w-sbk sg sg 1-f-gr 1-f-gr 0.5-f-sbk/gr 1-m-sbk

Profile

Horizon

Depth (cm)

0–6 6 – 10 10 – 22 22 – 40 40 – 60 60 – 80+ 0–6 6–7 7 – 11 11 – 23

D.E. Dahms / Geomorphology 42 (2002) 59–83

69

Table 2 (continued) Munsell Color Profile

Horizon

Morphostratigraphic Unit 5L 2Btb 3Cox1b 3Cox2b LC1 O E Bs1 Bs2 2Coxx 2Cu WL1 AO Ej Bw 2BCx 2Coxx 2Cu RFP1 A1 A2 Bw1 Bw2 Bw3 2BC1 3BC2 4Cox RFP2 A 2Bt1 2Bt2 2BC 2Cox

Depth (cm)

Moist

Dry

Texturea

Consistenceb

Structurec

23 – 29 29 – 75 75 – 85+ 0–3 3–6 6 – 18 18 – 45 45 – 80 80+ 0–5 5–9 9 – 30 30 – 52 52 – 68 68+ 0–5 5 – 13 13 – 24 24 – 32 32 – 59 59 – 92 92 – 120 120+ 0 – 13 13 – 23 23 – 50 50 – 60 60 – 75+

10YR4/4 10YR4/3 2.5Y4/4 – 10YR4/3 7.5YR4/6 7.5YR4/6 10YR4/4 5Y5/4 10YR4/3 10YR4/4 10YR4/6 10YR5/4 2.5Y5/4 5Y4/4 10YR2/2 10YR3/3 7.5YR3/4 7.5YR4/4 10YR3/6 10YR3/6 10YR4/4 2.5Y4/4 10YR3/2 10YR4/4 10YR4/6 10YR3/3 2.5Y4/4

10YR5/4 2.5Y6/4 2.5Y6/4 – 10YR5/3 7.5YR6/6 7.5YR6/6 10YR6/4 5Y7/4 10YR5/3 10YR6/4 10YR6/6 10YR6/4 2.5Y6/4 5Y7/2 10YR3/3 10YR4/3 7.5YR5/4 7.5YR5/4 10YR5/6 10YR5/6 10YR5/4 2.5Y5/4 10YR4/2 10YR5/4 10YR6/4 10YR6/4 2.5Y6/4

SL LS LS – SL SL SL SL SL LS L SL SL SL SL CL L SL SL SL LS SL SL L SL SL SL SL

ss-ps/vfr/so so-po/lo/lo so-po/lo/lo – so-po/vfr/so so-po/vfr/so so-po/vfr/so so-po/vfr/sh so-po/lo/lo so-po/lo/lo so-po/vfr/so ss-ps/vfr/so so-po/fi/sh so-po/fi/h so-po/lo/lo so-po/vfr/so so-po/vfr/so ss-ps/fr/sh ss-ps/fi/sh ss-ps/fi/sh so-po/vfr/so so-po/lo/lo so-po/lo/lo so-po/vfr/lo ss-ps/vfr/so ss-po/fr/so so-po/vfr/so so-po/lo/lo

1-m-sbk/gr sg sg 0.5-f-sbk 1-m-sbk 1-f-sbk 1-m-pl 2-m-abk sg sg 0.5-f-pl 1-m-sbk 2-f-abk 2-m-abk sg 0.5-f-sbk 1-m-sbk 1-m-sbk 1-m-sbk 1-m-sbk 1-m-sbk 0.5-f-sbk sg 1-f-sbk 1-m-sbk 1-m-sbk 1-f-sbk sg

a

Texture: SL, sandy loeam; LS, loamy sand; L, loam; S, sand; Si, silt; Cl, clay. Consistence: Wet—so, nonsticky; ss, slightly sticky; s, sticky; po, nonplastic; ps, slightly plastic; p, plastic. Moist—vfr, very friable; fr, fraiable; lo, loose; fi, firm; vfi, very firm. Dry—so, soft; lo, loose; sh, slightly hard; h, hard. c Structure: Grade—sg, single grain; .5, very weak; 1, weak; 2, moderate; 3, strong. Size—vf, very fine; f, fine; m, medium; c, coarse. Type—gr, granular; sbk, subangular blocky; abk, angular blocky; sg, single grain. b

B horizons varies from 22 to 47 cm. Profile RFP1 is not included as it is not developed in till.

there is a large eolian component in the soils (Dahms, 1993; Dahms and Rawlins, 1996).

4.3.1. Pedogenic silt and clay Soil profiles on older morphostratigraphic units in Stough Creek Basin generally contain more pedogenic silt and clay (total profile silt or clay, g/cm2) than do soils on younger units (Table 3). The largest amounts of clay often occur in A horizons of these soils, regardless of age. Overall, the means for pedogenic silt (whole profiles) are larger than those of clay (Fig. 5a). With time, amounts of pedogenic silt are greater than pedogenic clay (Fig. 5b). These trends suggest

4.3.2. Profile Development Index PDI values calculated for the Stough Creek Basin soils do not differentiate between units 1 and 2 (Table 3). PDI values increase noticeably for unit 3 soils but only weakly differentiate them from soils on unit 4. PDI values increase noticeably on unit 5. The limited number of soils developed on units 1 and 2 probably causes similarities among PDI values. The large boulder sizes on these units and limited quantity of fines with which to fill the large interstices limit the

70

Table 3 Laboratory data for soils: Stough Creek Basin Profile

Horizon

Depth

Particle size (%)

Pedogenic silt and clay (g/cm2)

% Grav

vol.% Grav

Bulk density (g/cm3)

Silt

Clay

Silt

Clay

Morphostratigraphic Unit 1 BFL9 Cox 0–5 Cu 5 – 25

84 84

12 11

5 5

42 56

27 46

1.35 1.77


0.14 0.00


0.08 0.00

Morphostratigraphic Unit 2 BFL8 Cox 0–5 Cu 5 – 25 SCB12 A 0–2 Cox 2 – 10 2Cu 10 – 30+

85 85 80 83 92

9 10 15 12 4

6 6 6 5 5

42 38 31 47 51

27 29 18 37 41

1.35 1.77 1.35 1.77 1.77


0.20 0.00 0.22 0.78 0.00


0.03 0.00
0.01 0.04 0.00

Morphostratigraphic BFL6 A 2Bt 2Cox1 2Cox2 BFL7 A 2Bw 2Cox1 2Cox2 SCB6 A Bt 2Cox1 2Cox2 SCB7 A Bw 2Cox1 2Cox2

Unit 3 0 – 10 10 – 20 20 – 28 28 – 45+ 0–7 7 – 15 15 – 30 30 – 45+ 0–5 5 – 17 17 – 30 30 – 50+ 0–5 5 – 15 15 – 25 25 – 50+

57 67 68 75 64 73 73 71 40 46 64 66 66 69 73 80

24 21 22 17 24 18 17 20 41 39 28 27 24 24 22 15

19 12 10 9 12 10 10 10 19 14 8 7 10 7 6 5

7 29 34 33 17 29 28 30 14 14 37 43 12 16 45 48

3 16 23 25 9 17 17 22 6 6 25 34 5 7 32 38

0.98 1.2 1.54 1.77 1.25 1.34 1.36 1.77 1.06 1.04 1.54 1.77 0.97 1.08 1.54 1.77

1.66 1.61 1.69 3.01 1.53 1.16 2.11 3.32 1.76 3.90 3.55 5.59 0.81 1.81 1.82 3.21

1.03 0.54 0.43 0.90 0.45 0.32 0.61 1.10 0.55 0.77 0.42 0.56 0.09
0.05 0.05 0.00

Morphostratigraphic Unit 4 BFL4 OA 0–5 Bt 5 – 13 2Cox1 13 – 37 2Cox2 37 – 63+

72 64 75 74

17 25 19 19

11 11 7 7

20 32 53 44

10 20 40 35

1.25 1.43 1.54 1.77

0.67 1.87 3.23 4.69

0.26 0.45 0.36 0.78

Profile Silt

Profile clay

PDI

Weighted PDI (85)

0.00

0

0.23

0.003

0.00

0

0.23

0.003

1.00

0.04

0.26

0.003

7.96

2.90

5.68

0.063

8.12

2.49

6.03

0.067

14.79

2.31

6.82

0.076

7.65

0.14

4.64

0.052

10.46

1.84

7.28

0.081

D.E. Dahms / Geomorphology 42 (2002) 59–83

Sand

Profile Development Index

BFL5

SCB8

SCB9

IL1

Morphostratigraphic BFL1 A Bt 2BC 2Cox1 2Cox2 BFL2 A AB Bt 2Cox1 3Cox2 BFL3 A AB Bt Cox1 2Cox2 SCB2 A Bt BC 2Cox

0–9 9 – 22 22 – 55 55 – 75+ 0–7 7 – 15 15 – 39 39 – 50+ 0–5 5 – 11 11 – 35 35 – 50+ 0 – 15 15 – 35 35 – 55 55+

63 64 70 83 49 55 84 83 62 62 69 80 48 53 70 72

23 24 20 12 35 32 14 16 26 29 30 20 33 30 23 20

14 12 10 5 15 13 2 0 12 9 0 0 19 17 7 8

22 31 32 46 11 15 51 59 8 22 25 45 8 25 40 43

9 18 22 36 5 7 38 49 3 10 16 35 3 13 28 34

0.94 1.26 1.62 1.77 0.99 1.1 1.54 1.77 1 1.09 1.54 1.77 1.03 1.17 1.54 1.77

1.25 2.75 6.68 1.90 1.92 2.17 2.35 1.27 0.97 1.36 8.11 2.73 4.01 5.09 4.23 1.88

0.40 0.85 1.99 0.11 0.47 0.42
0.87
0.44 0.18 0.08
1.51
0.77 1.64 2.07 0.27 0.40

Unit 5U 0–8 8 – 18 18 – 27 27 – 65 65 – 90+ 0–5 5 – 18 18 – 60 60 – 80 80+ 0 – 12 12 – 23 23 – 60 60 – 72 72+ 0–9 9 – 22 22 – 33 33 – 60+

57 63 80 61 78 57 66 64 75 78 65 64 58 65 78 59 59 66 84

28 20 16 30 16 25 20 23 18 16 20 22 31 24 16 22 26 23 11

14 17 4 10 6 18 14 13 7 6 15 15 11 11 6 18 15 10 5

8 20 40 43 53 14 15 29 30 53 11 18 24 36 53 16 17 20 51

4 11 25 29 43 6 8 18 20 43 4 8 13 25 43 7 8 12 41

1.21 1.27 1.32 1.45 1.77 0.97 1.26 1.47 1.54 1.77 1 1.04 1.25 1.54 1.77 1 1.2 1.38 1.77

2.14 1.70 1.01 9.99 3.08 0.86 2.30 9.40 2.47 0.00 1.53 1.62 11.85 2.78 1.25 1.35 3.18 2.52 2.11

0.71 1.21
0.21 1.52 0.38 0.44 1.06 3.91 0.39 0.00 0.80 0.76 1.96 0.82 0.14 0.86 1.26 0.58 0.20

12.58

3.35

10.93

0.121

7.71

0.89

6.35

0.071

13.16

0.26

6.6

0.073

15.22

4.38

11.59

0.129

17.91

3.82

11.88

0.132

15.03

5.80

18.34

0.204

19.03

4.48

17.61

0.196

9.16

2.90

10.46

0.116

D.E. Dahms / Geomorphology 42 (2002) 59–83

A 2Bt 2Cox1 2Cox2 A Bt 2Cox1 2Cox2 A 2Bt 2Cox1 2Cox2 A 2Bt 2BC 2Cox

(continued on next page)

71

72

Table 3 (continued) Profile

Horizon

Depth

Particle size (%)

Morphostratigraphic SCB3 A AB 2Bw 2Cox 2Cu SCB4 A Bt BC Cox 2Cu SCB5 A Bt 2BC 2Cox 2Cu SCB11 A Bt 2BC 2Cox1 2Cox2

Unit 1 0 – 10 10 – 26 26 – 48 48 – 65 65 – 80+ 0–7 7 – 20 20 – 43 43 – 55 55 – 65+ 0 – 10 10 – 25 25 – 52 52 – 62 62+ 0–9 9 – 20 20 – 30 30 – 45 45 – 55+

Morphostratigraphic Unit 5L SCB1 A 0–6 E 6 – 10 2Bs1 10 – 22 2Bs2 22 – 40 2Cox1 40 – 60 2Cox2 60 – 80+

Silt

Clay

vol.% Grav

Bulk density (g/cm3)

Pedogenic silt and clay (g/cm2) Silt

Clay

54 69 76 70 83 52 63 63 51 79 67 63 77 67 79 52 43 78 78 85

26 17 19 25 14 28 25 29 38 17 18 21 18 26 17 31 37 16 19 13

20 14 5 6 3 20 12 8 11 4 15 17 6 7 4 17 20 6 3 2

4 16 36 36 40 4 12 21 21 28 13 8 36 37 28 4 5 32 34 23

2 7 20 25 31 1 5 12 13 21 6 4 23 25 21 1 2 21 24 17

1.09 1.08 1.2 1.54 1.77 0.99 1.03 1.38 1.54 1.77 1.06 1.19 1.38 1.54 1.77 1 1.02 1.54 1.66 1.77

2.16 1.72 2.94 4.04 0.00 1.47 2.36 3.55 5.46 0.00 1.24 2.60 3.73 2.46 0.00 2.18 3.33 1.42 1.89 2.10

1.36 1.08
0.46 0.10 0.00 0.81 0.56 0.35 0.90 0.00 0.72 1.74
0.06 0.22 0.00 0.80 1.37 0.12
0.23
0.64

56 51 68 67 66 65

27 37 23 28 32 34

17 13 9 5 2 1

12 8 16 17 36 32

5 3 9 10 24 23

1.06 1.1 1.37 1.37 1.54 1.77

1.25 1.31 2.69 5.25 6.53 8.26

0.58 0.22 0.46
0.30
0.77
1.06

Profile Silt

Profile Development Index Profile clay

PDI

Weighted PDI (85)

10.86

2.54

10.66

0.118

12.85

2.62

9.2

0.102

10.02

2.68

11.65

0.129

10.91

2.29

9.32

0.104

25.30

1.26

11.62

0.129

D.E. Dahms / Geomorphology 42 (2002) 59–83

Sand

% Grav

SCB10

LC1

WL1

RFP2

0–6 6–7 7 – 11 11 – 23 23 – 29 29 – 75 75 – 85+ 0–3 3–6 6 – 18 18 – 45 45 – 80 80+ 0–5 5–9 9 – 30 30 – 52 52 – 68 68+ 0–5 5 – 13 13 – 24 24 – 32 32 – 59 59 – 92 92 – 120 120+ 0 – 13 13 – 23 23 – 50 50 – 60 60 – 75+

17 24 41 58 75 87 80 – 66 60 65 74 65 79 51 63 65 68 68 35 39 62 69 77 86 68 73 40 62 68 71 73

50 50 32 23 16 8 14 – 23 33 28 18 34 14 37 23 23 22 23 33 35 23 19 14 8 19 20 36 22 20 20 20

33 27 27 20 9 5 6 – 12 7 7 9 1 7 12 14 12 10 9 32 26 15 12 9 7 13 8 24 15 12 9 8

3 3 4 17 22 37 46 – 17 16 17 37 32 31 11 28 38 27 30 3 2 17 24 37 42 39 42 6 17 35 33 42

1 1 1 7 11 25 36 – 8 9 9 26 23 15 5 14 26 19 22 1 1 8 12 23 27 27 33 2 8 21 22 33

0.96 1.1 0.97 1.01 1.2 1.54 1.77 – 1.1 1.37 1.37 1.54 1.77 1.03 1.1 1.17 1.54 1.77 1.77 1.03 1.03 1.17 1.17 1.34 1.38 1.54 1.77 1.03 1.17 1.34 1.54 1.77

2.89 0.95 0.98 1.82 0.71 2.21 1.15 – 0.51 4.31 7.93 5.55 0.00 0.34 1.31 3.74 4.59 4.22 0.00 1.37 2.39 1.70 1.12 2.64 1.05 4.62 1.92 3.94 1.80 4.29 1.70 2.88

1.64 0.42 0.70 1.32 0.17
0.42 0.20 – 0.13 0.08 0.22 1.29 0.00
0.03 0.18 1.46 1.73 1.25 0.00 1.24 1.49 0.80 0.41 0.68 0.20 2.40 0.38 2.09 0.91 1.75 0.41 0.57

10.71

4.45

13.01

0.145

18.30

1.72

17.95

0.199

14.20

4.62

15.58

0.173

16.81

7.6

31.39

0.349

14.60

5.73

15.74

0.175

D.E. Dahms / Geomorphology 42 (2002) 59–83

RFP1

A Ej Bw 2ABb 2Btb 3Cox1b 3Cox2b O E Bs1 Bs2 2Coxx 2Cu AO Ej Bw 2BCx 2Coxx 2Cu A1 A2 Bw1 Bw2 Bw3 2BC1 3BC2 4Cox A 2Bt1 2Bt2 2BC 2Cox

73

74

D.E. Dahms / Geomorphology 42 (2002) 59–83

Fig. 4. Depths to the 2.5Y – 5Y hue (Cox-C) boundary of soil profiles described in Stough Creek Basin. Profile SCB10 is located in Helen Lake cirque, but is included in unit 5L as it is developed on what is interpreted to be the remnant of a Pinedale lateral moraine.

locations from which soil profiles can be described. No obvious topographic or geomorphic variables exist, however, to explain the minimal differences in PDI values between units 3 and 4. Erosion on the older deposit (unit 4) could be a factor, but this cannot be systematically demonstrated here.

5. Stratigraphic nomenclature and ages of the deposits 5.1. Nomenclature Interpretations of the post-Pinedale glacial succession for the WRR have focused chiefly on the age of the Temple Lake moraine (Table 4). Hack (1943) and Moss (1949, 1951) identified deposits here corresponding to two post-Pinedale glacial events. They identified the ‘‘Temple Lake moraine’’ as a pre-Altithermal unit as well as moraines corresponding to the ‘‘Little Glaciation’’ (Little Ice Age). Richmond revised their interpretations when he identified separate Temple Lake moraines (‘‘a’’ and ‘‘b’’) as representing the first two of three neoglacial (post-Altithermal) advances in the WRR and renamed the Little Glaciation the ‘‘Gannett Peak’’ (Richmond, 1962, 1965; Benedict, 1968; Birkeland et al., 1971). Currey (1974) presented a minimum-limiting age of 6500F230 14C years BP

from the base of a bog on the Temple Lake moraine to demonstrate a single Temple Lake moraine was deposited prior to the Altithermal and represented only the first of three separate post-Pinedale glacial episodes here. Miller and Birkeland (1974) concurrently described deposits corresponding to four post-Pinedale glaciations in the Temple Lake valley. They corroborated Currey’s pre-Altithermal age for the Temple Lake moraine and presented evidence for an additional unit intermediate between the Early Neoglacial and Gannett Peak deposits that they termed the ‘‘Audubonequivalent’’ (Table 4). Birkeland presented corroborating evidence for four post-Pinedale glacial events here from 14 alpine valleys and proposed new post-Pinedale stratigraphic units for the WRR (Birkeland, personal communication, 1998; Dahms and Birkeland, 2000). The revised unit names reflect localities in the WRR and are classified as Alloformations (North American Committee on Stratigraphic Nomenclature, 1983). This revision is included in Table 4 and is used in this study. 5.2. Correlations I assign morphostratigraphic units 1 –4 in Stough Creek Basin to the fourfold post-Pinedale glacial sequence presented for the WRR by Miller and Birkeland (1974) as revised by Dahms and Birkeland

D.E. Dahms / Geomorphology 42 (2002) 59–83

Fig. 5. Means of the total for pedogenic silt and clay (gm/cm2) in profiles on morphostratigraphic units mapped in Stough Creek Basin. Total pedogenic silt or clay is calculated for each profile as the sum of pedogenic silt or clay in all soil horizons above the C horizon. (a) Means of the total pedogenic silt and clay of the profiles on each morphostratigraphic unit. Simple linear plots illustrate the relation between pedogenic silt and clay over time and are not meant to portray best fit. Pedogenic silt apparently accumulates more quickly, indicating that eolian addition is important to soil formation here (see Shroba and Birkeland, 1983; Dahms, 1993; Dahms and Rawlins, 1996). In situ weathering may contribute more clay to the older soils, causing the increase in total pedogenic clay. (b) Mean accumulations of pedogenic clay in A versus B horizons of the soils (trends illustrated by natural spline curves). Clay accumulations in A horizons B horizons on units 1 – 3. Clay clearly becomes more abundant in B horizons only on older units (4 – 5L). As in (a), this pattern suggests weathering and translocation overcomes eolian addition only after a moderate period of time here. Eolian influx remains important at all times, as suggested by the higher silt content in the A horizons of progressively older units.

(2000; see Table 4). I assign morphostratigraphic unit 5 to the recessional Pinedale period. Morphostratigraphic unit 1 in Stough Creek Basin corresponds to the Gannett Peak Alloformation (ca. 500– 150 years BP). Unit 2 corresponds to the Black

75

Joe Alloformation, 2000 – 1500 years BP (Birkeland and Miller, 1989; Birkeland, personal communication, 1998; Dahms and Birkeland, 2000). The range of ages used here for the Black Joe deposits represents a composite of age estimates for pre-LIA deposits from the WRR and the Front Range (Mahaney, 1972, 1973; Benedict, 1973, 1985; Birkeland, 1973; Miller and Birkeland, 1974; Davis, 1988; Birkeland and Miller, 1989; Birkeland, personal communication, 1998) as few numeric ages have been presented for equivalent deposits in the Rocky Mountains. Unit 3 corresponds to the Alice Lake Alloformation and corresponds to the first glacial advance following the Altithermal (Hypsithermal as defined in Europe,

5000 14C year or 5600 cal. years BP; Porter and Denton, 1967). Age estimates for Alice Lake deposits (previously known as Early Neoglacial) are not well constrained in the WRR and estimates range from

6000 to 3000 years BP (Benedict, 1973; Birkeland, 1973; Andrews et al., 1985; Davis, 1988; Birkeland and Miller, 1989; Birkeland, personal communication, 1998; Dahms and Birkeland, 2000). Ages from the northern WRR (between ca. 5050 and 2760 14C years BP) are based on minimum-limiting ages from buried soils or organic matter (Mahaney, 1984a, 1987). No other numeric ages are directly associated with Alice Lake deposits in the WRR although recent AMS 14C ages from organics in sediment cores from the Temple Lake valley and Titcomb Lakes agree with the earlier interpretations of three neoglacial advances here (Gosse et al., 1999). Zielinski and Davis (1989) and Fall et al. (1995) place the beginning of neoglaciation at ca. 3300 14C years BP. Preliminary analyses of cores from upper and lower Titcomb Lakes (Gosse et al., 1999; Gosse, personal written communication, 2000) reveal as many as six post-Pinedale climate transitions may be recorded here. Thus, neoglaciation possibly began as early as 9500 – 8000 cal. years BP or as late as 6000 –5300 cal. years BP. Possible correlations exist between the Alice Lake Alloformation and the Triple Lakes deposits of the Colorado Front Range (Benedict 1967, 1968, 1973; Mahaney, 1984a; Birkeland et al., 1987). Davis notes a change occurs in the sedimentation regime, from massive to laminar, at ca. 5000 14C years BP in a core from Dorothy Lake, behind the Satanta Peak moraine in the Colorado Front Range (Davis, personal communication, 2000). He suggests the change represents

76

Table 4 Principal post-Pinedale stratigraphic correlations for the Wind River Range ka Moss, Richmond (1965) (1949, 1951), Holmes and Moss (1955) Little Glaciation

Gannett Peak

Currey (1974)

Miller and Birkeland (1974)

Late Neoglacial

Gannett Peak Gannett Peak Gannett Peak Gannett Peak

Temple Lake ‘‘a’’ 2

Audubon equivalent

Mahane (1984a,b)

Richmond (1986)

Audubon

Gannett Peak

Gannett Peak

Black Joe

Black Joe

Alice Lake

Alice Lake

Early Neoglacial

Indian Basin

4 6

Birkeland, Stough personal Creek Basin communication, (this study) 1998

Late Stade Pinedale

Indian Basin Moraine ?

8 Temple Lake

Temple Lake Late Pinedale Temple Lake

10 12

Temple Lake Donald Creek Temple Lake Temple Lake

Temple Lake Temple Lake

Temple Lake

Pinedale

Pinedale

Pinedale

Middle Stade Pinadale

14 16 18 20

22 24

Early Stade Pinedale

D.E. Dahms / Geomorphology 42 (2002) 59–83

Early Neoglacial

No data presented

Audubon

Temple Lake ‘‘b’’ Early Neoglacial

Zielinski and Zielinski (1989), Gosse et al. Davis (1987) Zielinski and (1995a,b) Davis (1989)

D.E. Dahms / Geomorphology 42 (2002) 59–83

the reformation of a glacier about this time. Elsewhere, Graf (1989) and Pederson (2000) report three episodes of aggradation in lakes of eastern Utah beginning at ca. 5000 14C years BP that represent the return of wet precipitation regimes following the early Holocene climatic optimum. Unit 4 corresponds to the Temple Lake Alloformation (Dahms and Birkeland, 2000). A preliminary exposure age on striated/polished bedrock on the riegel at Bigfoot Lake (Fig. 3) suggests this location was ice-free by 14,600F2100 10Be years BP (Dahms et al., 2000). This exposure age does not distinguish whether unit 4 was deposited during a pause in Pinedale deglaciation or by a re-advance following ice ablation to positions further upvalley. By correlating unit 4 with the Temple Lake Alloformation, I assign deposition of unit 4 to the Younger Dryas chron, ca. 12,800F200 to 11,500F500 cal. years BP (Zielinski and Davis, 1987; Alley et al., 1993; Gosse et al., 1995a, 1999).

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Morphostratigraphic unit 5 corresponds to the recessional period of the Pinedale glaciation (ca. <15,000 years BP). Recent work in the WRR places the Pinedale glaciation within oxygen isotope stage 2, between ca. 23,000 and 15,000 years BP (10Be, 26Al, 36 Cl ages reported by Gosse et al., 1995b; Chadwick et al., 1997; Phillips et al., 1997). Additional 10Be and 26 Al exposure ages on polished and striated bedrock on the floor of Stough Creek Basin suggest ice covered the lower basin until at least 13,000 years BP (Dahms et al., 2000). The highest deposits on the east basin wall (14,600 10Be years BP; Dahms et al., 2000; Fig. 3) may represent the level to which Pinedale ice filled Stough Creek Basin. These deposits correspond well to 10Be ages on polished-striated bedrock shown Pinedale ice was retreating from its terminal position in the lower Middle Papo Agie basin by 15,000 10Be years BP (Dahms et al., 2000). Thus, all other unit 5 deposits in Stough Creek Basin are considered to be Pinedale recessional deposits.

Fig. 6. Relations among lichen growth curves for Stough Creek Basin, the Colorado Front Range, Temple Lake valley, and Stroud Basin in the northern WRR. Regression lines are plotted only for the linear portion of each curve and do not reflect Beschel’s (1961) (Benedict, 1967, 1985, 1996). The curves for Stough Creek Basin and Temple Lake valley (Birkeland, personal communication, 1998) were constructed using the largest minimum diameters of R. geographicum s.l. thalli, while curves for the Colorado Front Range and Stroud Basin are based on the largest maximum diameters of R. geographicum s.l. thalli (Benedict, 1985, 1996; Mahaney, 1987). Calculated growth rates are as follows: Stough Creek Basin, 0.022 mm/year; 14 valleys of the middle and southern WRR, 0.024 mm/year; Front Range, 0.036 mm/year; Stroud Basin in the northern WRR, 0.038 mm/year.

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6. Comparison of Stough Basin RA data to other localities

Basin and the other valleys of the WRR are the minimum diameters of the largest thalli.

From the data presented above we may compare the glacial succession in Stough Creek Basin to those previously reported in other alpine valleys of the WRR. Similar techniques previously have been applied elsewhere in the WRR in the Temple Lake Basin (Miller and Birkeland, 1974) and in Titcomb, Indian, and Stroud Basins (Mahaney, 1978, 1984a,b, 1987). Birkeland (1973) noted that no single relative age-dating method is useful for dating glacial deposits. Indeed, no single method delineates all the postPinedale units at these localities. This remains the case in Stough Creek Basin and, thus, a number of similarities and differences exist among the RA data from Stough Creek Basin and those from other localities in the WRR.

6.2. Soil development Profile depth (depth to the Cox-C horizon boundary) and the PDI are the most useful RA parameters by which to compare Stough Creek Basin soils to other localities in the WRR and elsewhere in the Rocky mountains. 6.2.1. Profile depths I compared profile depths in Stough Creek Basin to those described by field and laboratory data

6.1. Lichen data The lichen cover estimates differentiate the Gannett Peak and Black Joe allostratigraphic units from the Alice Lake allostratigraphic units but are less robust for separating Alice Lake from Temple Lake deposits. The mean of the five largest thalli diameters adequately distinguishes all the post-Pinedale deposits. The increase in lichen cover estimates from Gannett Peak to the Alice Lake deposits reflects a pattern similar to that reported elsewhere in the WRR (Birkeland, personal communication, 1998; Dahms and Birkeland, 2000) and to that of Benedict (1967, 1968) in the Colorado Front Range. The average of the five largest thalli diameters from each unit in Stough Creek Basin (Table 1) are similar to those noted by Birkeland from other alpine valleys of the WRR (Birkeland and Miller, 1989; Birkeland, personal communication, 1998; Dahms and Birkeland, 2000). Lichen growth rates (Fig. 6) in Stough Creek Basin and other valleys of the middle and southern WRR are lower than those reported from the Front Range (Benedict, 1981, 1996) and from Stroud Basin in the northern WRR (Mahaney, 1987). The reason for this may simply be an artifact of sampling. Benedict and Mahaney measure the maximum diameter of the largest thalli while thalli diameters from Stough Creek

Fig. 7. Mean depths of soil profiles in Stough Creek Basin compared with those described by Birkeland from 14 cirque basins in the WRR (Birkeland, personal communication, 1998), Mahaney in Titcomb and Indian Basins (Mahaney, 1978, 1984b), and in Titcomb Basin (Hall, 1989). Bockheim (1980) (Birkeland, 1999) concludes that the equation [ Y = a + (b logx)] is the most appropriate chronofunction for many soil characteristics. The equation is fitted to each data set to visually compare the chronosequences. Soils on older stratigraphic units fit the equation more closely than soils on younger units. Soils below the curve are those on Black Joe deposits in Stough Creek Basin and Temple Lake valley where a lack of interstitial fines may have prevented complete sampling. The trend line constructed for Mahaney’s data would more closely correspond to the others if adjusted for the more recent age estimates and stratigraphic interpretations of Gosse et al. (1995a, 1999) and Zielinski and Davis (1987). Ages of soil parent materials used to plot data are as follows: 150 years for Gannett Peak deposits; 1500 years for Black Joe deposits; 4000 years for the Alice Lake deposits; 10,500 years for the Temple Lake deposits; 13,000 years for the 5U Pinedale recessional deposits; and 14,600 years for the 5L Pinedale recessional deposits.

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collected by Birkeland in 1972 – 1973 from 14 other cirque basins in the WRR (Birkeland, personal communication, 1998) and to Mahaney’s Titcomb Basin and Indian Basin soils (Fig. 7; Mahaney, 1978, 1984a,b; Hall, 1989). Mean depths of Stough Creek Basin soils are indistinguishable from those from Birkeland’s 14 cirque valleys. In Titcomb and Indian basins, Mahaney (1987) describes soils that are notably deeper than those reported either for Stough Creek Basin or those of Birkeland. Hall’s (1989) reinvestigation of Mahaney’s profiles, however, found many to be shallower than originally reported. It is, therefore, relevant here to note that recent 10Be exposure ages show all of Mahaney’s ‘‘Early Neoglacial’’ and ‘‘post-Pinedale’’ moraines in Titcomb Basin are >10,000 10Be years BP (Gosse et al., 1995a, 1999). Thus, soils developed on Mahaney’s (1984a) Early Neoglacial (also known as Indian Basin) moraines cannot be considered to have developed on post-Altithermal deposits. If Mahaney’s data are assigned to sequentially older units, then the data falls closer to the regression lines developed for all other localities in the WRR (Fig. 7). The combination of numeric ages and soils data suggests, therefore, that the stratigraphic positions of Mahaney’s Gannett Peak, Audubon, and Indian Basin deposits

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may correspond, respectively, to the Black Joe, Alice Lake, and Temple Lake alloformations. I reinvestigated soil TB-15 on Mahaney’s (1978) ‘‘Gannett Peak’’ moraine in 1997 and found the profile depth to be similar to Mahaney’s description ( 20 cm). This A/Cox/C profile is most comparable, however, to the soils described on the Black Joe alloformation in Stough Creek Basin and elsewhere in the WRR (Birkeland, personal communication, 1998; Dahms and Birkeland, 2000). Since Gosse et al.’s exposure ages place Mahaney’s Audubon units at >10,000 years BP, it is possible that the moraines in Titcomb Basin that correspond to the Gannett Peak and Audubon advances have not been identified correctly, possibly due to the depth of perennial snow cover. 6.2.2. Profile Development Index The present data for Stough Creek Basin (Table 3) are the first PDI calculations published for the WRR alpine region. Birkeland et al. (1987) reported PDI values from Arapaho cirque in the Indian Peak area of the Colorado Front Range that represent relatively high rates of soil development, compared to the Stough Creek Basin soils (Fig. 8). Weighted PDI values are based on the same profile depths (85 cm) and indicate soil development in the Front Range may

Fig. 8. Plot of the weighted Profile Development Index (PDI) values versus approximate age of soil parent materials in Stough Creek Basin and the Colorado Front Range. All PDI values are based on 85-cm thick soil profiles (Table 2, this study; Birkeland et al., 1987). Trend lines suggest that soils develop more rapidly in the Front Range than in Wyoming. This pattern may be due to climate differences between the Front Range and the southern WRR (which is mostly surrounded by semi-desert), although Birkeland et al. (1989) and Birkeland (1999) observed that many characteristics of soils in the WRR are similar to that of the Front Range.

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proceed at rates of 2 –3 those in the WRR. When we compare climate data between these areas, we see that MAT in the Front Range is nearly 3 °C warmer than that of the WRR (
3.8 vs.
6.9 °C; Birkeland et al., 1987; Naftz and Miller, 1992). Birkeland et al. estimate the MAP in Arapaho cirque (Ft. Range) to be 102 cm/year, which is within the range of wet deposition reported for Black Joe Lake in the southern WRR (Galbraith et al., 1991). Mahaney (1978) used lapse rate estimates to calculate precipitation in the northern WRR is 400 mm/year. The lower precipitation estimate for the WRR appears more realistic since elevations in the WRR are generally lower than those of the Front Range and the southern WRR is surrounded by high semi-desert basins. Thus, the colder/drier climate estimated for the WRR apparently is reflected in the smaller PDI values.

7. Conclusions RA data collected from glacial deposits in Stough Creek Basin, WY, indicate that the glacial succession here includes five allostratigraphic units (North American Committee on Stratigraphic Nomenclature, 1983; Birkeland, personal communication, 1998; Dahms and Birkeland, 2000). These data indicate the mean diameters of lichen thalli (R. geographicum s.l.), and the depths of soil profiles (Cox-C boundary) are the most robust data to indicate relative age in this basin. Pedogenic clay and the PDI (Harden, 1982; Birkeland et al., 1991a,b) are less robust but still useful RA data here. The RA data indicate that the five morphostratigraphic units described here correspond to discrete allostratigraphic units previously recognized in the WRR (Birkeland, personal communication, 1998; Dahms and Birkeland, 2000). Morphostratigraphic unit 5 corresponds to the recessional Pinedale period (<15,000 years BP). Stratigraphic units 4 through 1 represent post-Pinedale glacial advances. Units 4 – 1 correspond to the Temple Lake (10 –12 ka), Alice Lake ( 5500 –4000 ka), Black Joe (2000 – 1500 years BP), and Gannett Peak (350 – 100 years BP) alloformations, respectively. Interpretations of the climatic variability that these deposits represent are based only on the assumption that the four alloformations represent four periods in Stough Creek Basin since the Pinedale glacial max-

imum during which ELAs were lower than at present. That a series of four post-Pinedale glacial deposits is identified in 14 other cirque basins of the WRR and four sedimentation sequences are identified in lake sediments collected from the Temple Lake valley and from Titcomb Basin (Zielinski and Davis, 1989; Gosse et al., 1999) suggest climate variability since the last glacial maximum has been relatively synchronous throughout the WRR. Deposits corresponding to the Temple Lake Alloformation in Titcomb Basin, Stough Creek Basin, and elsewhere now appear to be well constrained to represent a pre-Altithermal climatic event (Younger Dryas) in the WRR. The lack of tightly constrained 14 C ages for Neoglacial deposits in the WRR and the apparent asynchroneity among lake-core 14C ages in the WRR and between the WRR data and that of the southern Rocky Mountains and nearby Great Basin locales illustrate the magnitude of information left to be discovered concerning the climatic significance and timing of post-Altithermal events in the Rocky Mountain region.

Acknowledgements This project was partially funded by 1994 and 1996 Summer Fellowships from the Graduate College of the University of Northern Iowa. The University of Missouri Department of Geology graciously provided field support at Camp Branson. P.W. Birkeland provided boulder weathering estimates and supplementary lichen cover estimates during a visit to the basin in July 2000. Allyson Anderson provided field assistance in 1996. Mike Applegarth performed the bulk density analyses. A special-use permit from the US Forest Service allowed sampling in the Shoshone wilderness. Preliminary cosmogenic age determinations are part of a project sponsored by NSF grant SBR-9631437 to J. Harbor, the late L. Horn, D. Dahms, L.A. James, and D. Elmore. Derek Fabel provided preliminary exposure ages and the background contours for Fig. 3.

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