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Soil science (particularly pedology) and archaeology are closely allied in their temporal and spatial scales, and among the earth sciences, pedology is most similar to archaeology in operational and processual scales. These similarities in scale are apparent in both regional and site-specific studies. At large (regional) scales, soil stratigraphy has long been used in archaeology for correlating sites and for dating. Soil-geomorphic investigations also are compatible in scale to regional archaeological investigations, focusing on dating, environmental reconstruction, and landscape evolution. Soil micromorphology (soil petrography) is also useful for regional geomorphic and archaeologic studies, including investigations of sediment provenance, landscape evolution, environmental reconstructions, and agricultural development. At small (site-specific) scales, the focus of pedology—the soil profile—is similar in scale to many archaeological sites (tens of centimeters to a few meters thick) and the scale of many pedological features is similar to that of archaeological features (a few millimeters to tens of centimeters). Soil variability at small scales as a function of slope, drainage, or lithologic change is a common theme in pedology and is also of archaeological significance for stratigraphic correlation and interpretation of site formation processes. Temporal scales of formation of individual pedogenic versus anthropic features are disparate (centuries to millennia versus days to decades, respectively), but overall processes of site formation and cultural evolution operate at temporal scales similar to those of soil formation (decades to millennia). The scalar compatibility of archaeology and pedology strongly argues for pedologists and pedologic perspectives to be involved in all phases of archaeological research.

Abstract The Southern Great Plains physiographic sub-province lies south of the Cimarron River, which crosses the plains at ~37° N latitude (Fig. 1). The sub-province is bounded on the west by the Southern Rocky Mountains Province and Sacramento section of the Basin and Range Province. On the east the Great Plains are bounded by the Caprock Escarpment and are separated from the Gulf Coastal Plain by the Balcones Escarpment. The southern Great Plains physiographic sub-province is divided into the Pecos Valley and Raton sections on the west, the High Plains section on the east, and the Edwards Plateau on the south. “In the public mind the Great Plains are thought of as a vast monotonous plain that lacks scenic interest, but has to be crossed to reach the scenic Rocky Mountains to the west“ (Thornbury, 1965, p. 287). Whereas this region clearly lacks areas of high relief and thus scenic wonders, it does contain some of the most extensive deposits of Tertiary and Quaternary sedimentary and volcanic rocks that have been recognized in North America. These units are commonly well exposed along the banks of stream systems being incised into the Great Plains and in the high scarps that bound the High Plains. Numerous descriptions of the Quaternary geology and geomorphology of the Southern Great Plains have been published since the first reports became available late in the 19th and early 20th centuries (Johnson, 1901; Baker, 1915). Of these, useful reviews or

Abstract Most archaeologists recognize that a relationship exists between the cultural remains they find in the ground and the soils. Beyond that simple relationship, however, archaeologists' understanding of what can be learned from soils and indeed what a soil is and is not varies tremendously. In general, the applications of soil studies in archaeology are either very large scale, such as the capability of regional soils to support agriculture or use of soils as stratigraphic markers, or very small scale, for example, studying the particle-size distribution or chemistry of a soil. There is a significant middle ground in soil studies that is often overlooked. This involves investigation of soils as three-dimensional bodies intimately related to the landscape, focusing on their classification and genesis. This study of soils and their natural setting is a part of soil science called "pedology." The aspect of pedology most directly related to archaeology evolves from Quaternary geology and geomorphology (rather than agriculture) and sometimes is referred to as soil-geomorphology (e.g., Ruhe, 1983; Birkeland, 1984; Catt, 1986). This chapter will review basic aspects of pedology, and how they apply to archaeology in North America. There is considerable literature concerning the use of soils in archaeological investigations. Much of the initial, substantive work was done in Great Britain (e.g., Cornwall, 1958, 1960), establishing a tradition that continues (e.g., Limbrey, 1975; Shackley, 1981). In North American archaeology, soils were originally used primarily as stratigraphic markers and continue to be so used with considerable success (e.g., Judson, 1953; Haynes, 1968,

Abstract Begin in Crosbyton, Texas (Fig. 1). Take U.S. 82 west 35 mi (56 km) to Lubbock. On the northeast side of Lubbock at the intersection of U.S. 82 (which is also U.S. 62 along this stretch of the road) and Loop 289, turn right (north) off of U.S. 82 and follow Loop 289 to the north and west. Cross over I-27/U.S. 84, and take the University Avenue exit. Stay on the frontage road and continue west, parallel to the loop. Cross University Avenue and continue west with the large Texas Instruments (TI) plant to the north (right). Just past the TI plant the road drops into Yellowhouse Draw. The Lubbock Lake site, is in the trees to the northwest, about 300 ft (100 m) away. On the floor of the draw, take the only paved road north (right). Follow it for 0.3 mi (500 m) as it curves to the left along the edge of the draw. A chain-link fence enclosing most of the trees becomes visible. This is Lubbock Lake.

Abstract Blanco Canyon and Mount Blanco are located along the eastern Caprock Escarpment of the Southern High Plains (Llano Estacado) in the Texas Panhandle near Crosbyton, Texas. The Blanco Canyon exposures are along U.S. 82 where it crosses lower Blanco Canyon east of Crosbyton (Fig. 1). Within a distance of 5.5 mi (8.9 km), the highway descends from the High Plains through the Bridwell and Couch Formations (Ogallala Group) to Triassic red beds before climbing back onto the High Plains surface. The route passes near the Bridwell and Couch type sections and is flanked by several excellent roadside exposures. Outcrops at four Blanco Canyon localities are discussed in this chapter. Collectively, they document the buildup and subsequent dissection of the Southern High Plains since late Miocene time. Mt. Blanco can be reached by traveling north from Crosbyton on Farm Road 651 across the High Plains surface (Backwater Draw Formation). At 7.8 mi (12.5 km) the road descends into Blanco Canyon. Below the escarpment the highway crosses the mouth of Crawfish Creek, a major reentrant of Blanco Canyon. As the road descends the side of the canyon, the white beds of the Blanco Formation are apparent to the left and right just below the reddish sands of the Backwater Draw Formation. After descending into the canyon, turn left (west) on Farm Road 193 and drive 0.7 mi (1.1 km) to Mt. Blanco, which is the conical erosional remnant on the south side of the road.

Abstract The Great Plains Physiographic Province (Fig. 1) is a generally north-south band of the western interior of North America, subcontinental in scale, that averages about 600 km in width and extends from northwestern Canada through the United States to the border with Mexico. With tongue-in-cheek, Thornbury (1965, p. 287) claimed that “in the public mind the Great Plains are thought of as a vast monotonous plain that lacks scenic interest, but has to be crossed to reach the scenic Rocky Mountains to the west.” It is generally true that the Great Plains, and especially the High Plains, have low relief. But there are many scenic exceptions, largely areas of negative relief along the eroded margins of the plains and in river valleys. Areas of positive relief include structural highs such as the Black Hills (Fig. IB) and other outliers of the Rocky Mountains. These areas of positive and negative relief are especially important, because they contain the sections where the geologic and geomorphic history of the Great Plains is best exposed.