Kpy – Yellow Mounds Paleosol equivalent: Terry (1993, 1995a), Terry and LaGarry (1994), and Terry and others (1995) correlated this unit into Nebraska from southwestern South Dakota, It consists of pedogenically altered Pierre Shale, and varies in color from yellow to ochre, orange, pink, and white. The original fissility of the parent shale is almost entirely overprinted by pedogenic features, which include root traces, ped structures, cutans, mottling, pedogenic silcretes, calcareous nodules, and redoxymorphic iron concentrations and nodules. APedogenic limonite frequently occurs 1-2 m below the weathered upper surface. Diagenetic gypsum is also present 1-2 m below the weathered upper surface where overlain by depositional gypsum in the Peanut Peak Member of the Chadron Formation [Wolf Butte (Nebraska) 7.5’ quadrangle: LaGarry and LaGarry (1997n)]. This unit is 1-15 m thick across the northern part of the study area. Like its parent material, it typically weathers as low hummocks or as steep escarpments in cutbanks of streams. Outcrops of this unit are frequently covered by cobble lag (stippled on maps) remnant of the overlying Chamberlain Pass Formation. Its contact with the overlying Chamberlain Pass Formation is a regional unconformity. Its contact with the underlying unaltered Pierre Shale is gradational. Although this unit is stratigraphically equivalent to Retallacks (1983) Yellow Mounds Paleosol Series, which was first described in the Big Badlands of South Dakota, it likely represents a different soil series. This unit corresponds to the lower part of Schultz and Stout’s (1955) “Interior Paleosol Complex”. Qa1 Youngest alluvium (Holocene)- Commonly sand and pebbly gravel, minor thin sandy silt beds: yellowish-gray and yellowish-orange; unit underlies the modern stream channels and floodplain. Sands are trough and planar bedded. Most clasts are derived from local bedrock. Commonly 1-4 m thick. Qa2 Older alluvium (upper Pleistocene)- Pebbly gravel and sand and local beds of silt. Deposit underlies a terrace in the southwest corner of the quadrangle about 25-30 m above the North Platte River. Qa3 Older alluvium 1 (Pleistocene) Clays to cobble sized sediment deposited in modern and ancient stream channels and floodplains. Qa4 Older alluvium (lower Pleistocene)- Pebbly gravel and sand; pale orange and grayish orange; occurs 75 to 115 m above the North Platte River. Commonly 5-20 m thick Qr1 – Clayey Residuum: This unit consists of residuum and soils derived from the weathering of the Pierre Shale and minor amounts (10%-15% of alluvial and colluvial clay sediments. This unit is mapped based on exposures in cut banks and the distribution of soils of the Pierre-KyleSamsil association (Ragon and others, 1977). Residuum or soil < 5 cm thick is mapped as Pierre Shale. This unit typically has a gradational contact with adjacent Qr2 and Qr3. Qr2 Silty residuum (Pleistocene) Residuum and soils derived from the weathering of silty claystones, clayey siltstones and siltstones of the White River Group and minor amounts (10-15%) of alluvial and colluvial silty clay sediments. Qr3 Sandy residuum (Pleistocene) Residuum and soils derived from the weathering of sandy siltstones and sandstones of the White River and Arikaree groups and minor amounts (1015%) of alluvial and colluvial silt and sand sediments. Twbo – Brule Formation, Orella Member: This unit consists of thinly interbedded brown, orange, and buff volcaniclastic clayey siltstones, volcaniclastic silty claystones, discontinuous medium to coarse grained, crossbedded and massive, brown sheet sandstones, and multistoried basal channel sandstones. The clayey siltstone, silty claystone, and sheet sandstone beds usually occur as couplets <0.5 m thick, with each couplet consisting of a thin, discontinuous sheet sandstone and an associated pedogenically altered clayey siltstone or silt claystone. The only pedogenic features with the silty claystone and clayey siltstones consist of chalcedony-filled root voids and insect tunnels. Terry and others (1995) described these weakly developed paleosols as “entisols”. The distribution of the discontinuous sheet sandstones is controlled by a complex overlapping cut-and-fill geometry (see Wells, 1994; Wells and others 1994, 1995; Terry and others, 1995; LaGarry and LaGarry, 1997n). The sheet sandstones are thinnest, poorly developed, or absent in the basal one-third of the paleovalley fills (Wells, 1994; Wells and others, 1995). Common sedimentary structures within these sheet sands include soft sediment deformation, fluid escape structures, planar crossbeds, mudcracks or subaqueous shrinkage cracks, and invertebrate trace fossils (Terry and others, 1995; Wells and others, 1995). These “nodular” appearing sheet sands were interpreted as pedogenic nodules by earlier workers (Schultz and Stout, 1955; Schultz and others, 1955). A 0.01 m thick volcanic ash bed (the “Serendipity Ash”) occurs 16 m above the base of the unit at the level of Schultz and Stout’s (1955) “Diplolophus insolens bench”. The basal multistoried channel sandstone (the “Toadstol Park Channel complex” of Schultz and Stout, 1955) is 0-9 m thick, and consists of overlapping paleochannels with trough and planar crossbedded, medium to coarse grained, clay matrixsupported sandstones having a gravel lag, thinly bedded and laminated green sandstones, and trough crossbedded conglomeratic sandstones having a gravel lag that contains small fragments of vertebrate bone and turtle carapace. These basal sandstones contain a suite of sedimentary structures consistent with a “mixed” braided/meandering river system, including trough crossbeds and lateral accretion surfaces (Terry and others, 1995). They are exposed intermittently within the Roundtop (Nebraska), Horn (Nebraska), Bodarc (Nebraska), and Warbonnet Buttes (Nebraska) 7.5’ quadrangles (see also LaGarry and LaGarry, 1997a). The uppermost surface of the “Toadstool Park Channel complex” contains abundant vertebrate and invertebrate trace fossils, including tracks and trails of worms, insects, crustaceans, birds, rhinoceroses, entelodonts, camels, rodents, lagomorphs, oreodonts, and carnivores (Nixon and LaGarry-Guyon, 1993a, 1993b; Terry and others, 1995). Vertebrate fossils are common within the silty claystones and clayey siltstones. The overall thickness of this unit is 26-29 m, and it weathers into steep, step-and-riser badlands. This unit thins to the east [Chadron West (Nebraska) 7.5’quadrangle] and west [Sherrill Hills (Wyoming-Nebraska) 7.5’ quadrangle] to 2-4 m of thinly bedded buff or brown siltstone. This unit thins to the east [Chadron West (Nebraska) 7.5’quadrangle] and west [Sherrill Hills (Wyoming-Nebraska) 7.5’quadrangle] to 2-4 m of thinly bedded buff or brown siltstone. This unit has an intertonguing contact with the overlying Whitney member, except where incised by paleochannels within the lower Whitney Member. It has an intertonguing contact with the underlying “Big Cotton wood Creek member” of the Chadron Formation, except where the underlying Chadron Formation is incised by the “Toadstool Park Channel complex.” This unit is equivalent to Schultz and Stout’s (1955) “Orella B” and “Orella C.” Twc1 – Big Cottonwood Creek Member: This new lithostratigraphic unit (Terry and LaGarry, 1998) is named for prominent exposures along Big Cottonwood Creek near Toadstool Geologic Park [Roundtop (Nebraska) 7.5’ Quadrangle: LaGarry and LaGarry (1997); see also Terry and others (1995)]. It consists primarily of pedogenically altered volcaniclastic silty claystones and minor amounts of interbedded claystone, pedogenic carbonate, lacustrine carbonate, massive lenticular sandstone, cross and planar bedded sandstone, diagenetic and sedimentary gypsum, volcanic ash, and a multistoried basal channel sandstone. Weakly developed paleosols in its uppermost 20 m give this unit a characteristic banded appearance; common colors are yellow, buff, pink, tan, green and red. The lowermost 15-20 m has less paleosol development, with common colors being green, yellow and red. In addition to carbonates (typically calcretes), pedogenic features within this unit include ped structures, cutans, and root traces ( Terry, 1995b). The pedogenic carbonates are <0.5 m thick and lenticular or tabular. Many contain fossilized dung rolled into balls by insects prior to deposition. The lacustrine carbonates are thin(<0.3 m thick), tabular, and discontinuous, and contain algal laminae, ostracodes, plant macrofossils, and fish remains (see also Welzenbach and Evans, 1992). Lacustrine carbonates with a high silt or clay content are considered marls (Terry and others, 1995; LaGarry and LaGarry, 1997). The massive and planar bedded sandstones have a wide geographic distribution (see LaGarry and Terry, 1997). However, most of the diagenitic gypsum (often occurring as psuedomorphs) and all of the sedimentary typsum (beds 0.2-0.6 m thick0 are restricted to the Wolf Butte (Nebraska) 7.5’ quadrangle (LaGarry and LaGarry, 1997n). The gypsum, sandstone, limestone, marl, and claystone beds are most common within the lower 15-20 m of the unit. Multistoried basal sandstones 2-5 m thick occur locally [Sherrill Hills (Nebraska), Story (Nebraska), and Story NE (Nebraska), and Roundtop (Nebraska) 7.5’ quadrangles: see also LaGarry and LaGarry (1997)]. At least five prominent volcanic ashes are present throughout this unit. The uppermost ash, Schultz and Stout’s (1955) “upper purplish-white layer” is locally widespread marker bed. The next lower ash, Schultz and Stout’s (1955) “lower” or “second purplish-white layer” is less widespread, and often only slightly more vitric than the adjacent volcaniclastic silty claystones. The lower three ashes are lenticular and really restricted, occurring within paleovalleys incised into the underlying Peanut Peak Member. The lowermost 20 m of this unit typically occurs as isolated erosional remnants within these paleovalleys [Horn (Nebraska) 7.5’ quadrangle]. This unit is calcareous in zones, giving it a nodular (5-10 cm diameter) appearance. It is also highly fossiliferous, containing abundant fossil vertebrate and infrequent fossil invertebrate remains. The overall thickness of this unit is 22-40 m; it is thickest where it has incised into the underlying Peanut Peak Member. This unit typically weathers into smooth, near vertical faces and badlands. It has an intertonguing contact with the overlying Brule Formation, except where it is incised by the “Toadstool Park Channel complex” of the Orella Member of the Brule Formation. It has an intertonguing contact with the underlying Peanut Peak Member, except where this unit incises or fills valleys and depressions in the underying Peanut Peak Member. This unit is equivalent to Schultz and Stout’s (1955) “Chadron B3”, “Chadron B4”, “Chadron C”, and “Orella A”. This unit does not occur east of the Trunk Butte (Nebraska) 7.5’ quadrangle, where this stratigraphic position is occupied by the “Trunk Butte beds” of the Chadron Formation (LaGarry and LaGarry, 1999). Twc2 – Chadron Formation, Peanut Peak Member: Terry (1995, 1998), Terry and LaGarry (1998), and Terry and others (1995) correlated this unit into Nebraska from southwestern South Dakota. It consists of dark olive, gray, yellow and red claystones. Most primary sedimentary structure within the claystones (e.g., lamination) are overprinted by pedogenic features, which include root traces, ped structures, cutans, mottling, and calcareous nodules. Discontinuously bedded gypsum, lacustrine limestone and marl, pedogenic calcrete, and sandstone beds occur in different locations and at various stratigraphic levels within the unit. Gypsum beds occur as diagenetically emplaced (0.1-0.5 m thick) and as a result of primary deposition (0.1-0.25 m thick) [Wolf Butte (Nebraska) 7.5’ quadrangle: see LaGarry and LaGarry (1997)]. Lacustrine limestones are tabular (0.05-0.25 m thick), are widespread both geographically and stratigraphically, and contain algal laminae, ostracodes, plant macrofossils, and fish remains (see also Welzenbach and Evans, 1992). The calcretes are restricted to the Horn (Nebraska), Trunk Butte (Nebraska), and Chadron West (Nebraska) 7.5’ quadrangle (see also LaGarry and LaGarry, 1997; LaGarry and Terry, 1997). Isolated sandstones are massive, lenticular or tabular, crossbedded, gypsiferous (0.1-1.5 m thick), and occur west of Toadstool Park [Roundtop (Nebraska) 7.5’ quadrangle: LaGarry and Terry (1997)]. At least one, and possibly as many as four lenticularly bedded vocanic ashes (0.1-0.3 m thick) are present throughout the unit. This unit has a thickness of 2-17 m. Its contact with the overlying “Big Cottonwood Creek member” is intertonguing except where incised by the basal channel sandstones of the “Big Cottonwood Creek member” or eroded into paleovalleys. Its lower contact with the underlying Chamberlain Pass Formation is a regional unconformity. This unit weathers into smooth, low hummocks, and is equivalent to Schultz and Stout’s (1955) “Chadron B1” and “Chadron B2”, and Clark and others’ (1967) “Chadron Formation undifferentiated” and Peanut Peak Member of the Chadron Formation in the Big Badlands of South Dakota. Twc3 – Chadron Formation, “Trunk Butte member” This provisional lithostratigraphic unit (LaGarry and LaGarry, 1999) is named for prominent exposure in the flanks of Trunk Butte, 14.5 km west of Chadron, Nebraska [Trunk Butte (Nebraska) 7.5’ quadrangle]. It consists primarily of medium to thickly bedded, pedogenically altered brown, pink, red, green and olive silty claystone and clayey siltstone microbreccias interbedded with prominent ledge forming calcretes, lenticular pockets of trough crossbedded green silts and fine sand, pedogenically altered brown claystones, and volcanic ash. The calcretes dominate this unit. They are 0.1-5 m thick, and account for as much as 60% of the exposed strata. In addition to the prominent calcretes, pedogenic features include root traces, mottles, peds, cutans, and worm casts and voids. Fifteen meters above the base of the section is a horizon consisting almost entirely of fossil dung rolled into balls by insects prior to burial. Two volcanic ashes are exposed 6 and 13 m above the base of the section. The lower ash is a lens 0-2.5 m thick. The second is only 0.1 m thick, but has a characteristic blue color. Skinner (unpublished field notes 1956-1964, archived at the Division of Paleontology, University of Nebraska State Museum) correlated these ashes to Schultz and Stout’s (1955) “lower purplish-white” and “upper purplish-white” layers, respectively. This unit is about 22 m thick at the proposed type section at Trunk Butte, and up to 5 m is exposed within cut banks to the west [Chadron West (Nebraska) 7.5’ quadrangle]. Its upper contact is a local erosional unconformity underlying thinly bedded pale brown siltstones of the Orella Member of the Brule Formation. The lower contact is an erosional unconformity where this unit has incised or filled valleys and depressions within the underlying Peanut Peak Member of the Chadron Formation. This unit is the equivalent to Skinner’s “Trunk Butte member” of the Chadron Formation, and part of the “Big Cottonwood Creek member” as originally defined by Terry and LaGarry (1998). Twcp – Chamberlain Pass Formation: Terry (1993, 1995a), Terry and LaGarry (1994), and Terry and others (1995) correlated this unit into Nebraska from southwestern South Dakota. It consists of pedogenically altered red, gray, white, yellowish olive, and olive silty claystones and interbedded lenticular single and multistoried white, gray, yellow, yellowish green, or green trough crossbedded channel sandstones. The claystones [“mudstones” of Evans and Terry (1994) and Terry and Evans (1994)] are laminated or massive and typically 1-3 m thick. The claystones contain Terry’s (1993, 1995a) dark red Interior Paleosol Series equivalent (see Retallack, 1983) and yellowish olive Weta Paleosol Series equivalent (see Evans and Terry, 1994; Terry and Evans, 1994). Most primary sedimentary structures (e.g., lamination) are overprinted by pedogenic feature, which include root traces, ped structures, cutans, mottling, pedogenic silcretes, calcareous nodules, and redoxymorphic iron accumulations. Calcareous nodules (2-5 cm diameter) occur in descrete horizons. The sandstones are single (0.5-1.0m thick) and multistoried (2-8 m thick), fine to coarse grained, pedogenically altered, and usually contain a gravel to cobble sized lag at base. Pedogenic alteration of the sandstones has transformed their feldspars into kaolinitic clays, an based on the amount of kaolinite within these sandstones, they were likely arkosic when deposited (Terry and Evans, 1994). Individual sandstone bodies are trough crossbedded, fine upwards, and contain pebble stringers, intraclasts, and large blocks of reworked red and yellowish olive claystone and shale incorporated into their base. The overall thickness of this unit is 1-13 m. Its contacts with the overlying Chadron Formation and the underlying Yellow Mounds Paleosol Series equivalent are regional inconformities. Along Whitehead Creek in the Five Points (Nebraska), Montrose (Nebraska), and Roundtop (Nebraska) 7.5’ quadrangles (see also Terry and others, 1995; LaGarry and LaGarry, 1997n) this unit had incised into underlying unaltered Pierre Shale. The claystones weather into low, smooth hummocks, and the channel sandstones weather into ledges and vertical cliffs. This unit corresponds to the basal gravels and “beds of a bright dark red color” of Darton’s (1899) original Chadron Fromation, the upper part of Schultz and Stout’s (1955) “Interior Paleosol Complex” (the Interior Paleosol Series equivalent), and Schultz and Stout’s (1955) “Chadron A” or “Yoder” (the channel sandstones: Terry and others, 1995; LaGarry and LaGarry, 1997n).