This study examined the depositional environment of the Brushy Basin Member (Jurassic Morrison Formation) in a small (< 2 km2) area in east-central Utah because of a controversy regarding the origin of several significant dinosaur sites. Previous interpretations place the depositional environment to have resulted from either a fluvial crevasse splay-fill or a fluvial delta prograding into a large lake (Jeffery et al., 2004) and (Jeffery et al., 2005). This study found the Brushy Basin Member to consist of stream deposits, including single-story and multi-story channel-fills, lenticular abandoned channel-fills that are interpreted as the positions of former oxbow lakes, extensive overbank mudstones, and paleosols of various degrees of development. The fluvial architecture in this relatively small (approximately 2 km2) area, which contains several dinosaur quarries of significant bone accumulation, was ascertained from a north-south transect of 10 stratigraphic sections. Six of the stratigraphic sections (each approximately ~80 m thick) begin at the contact of the Salt Wash Member-Brushy Basin Member and terminate within the Brushy Basin Member at a distinct mudstone color change which also represents a significant change in fluvial architecture in the upper portions of the Brushy Basin Member. The single-story fluvial channel-fills consist of fining-upward sequences of basal scours, channel lag deposits (lithofacies Gm), cross-bedded conglomerate and sandstone (lithofacies Gt, Gp, St, and Sp), sandstone with intraclasts (lithofacies Se), ripple-laminated sandstone (lithofacies Sr), and massive sandstones (lithofacies Smc and Smf). These sequences are arranged in lateral accretion surfaces which are interpreted to represent meandering stream point bar and pool deposits, with an average paleo-channel depth of 1-3 m and width approximately 10-20 m. Proximal and distal overbank sequences produced as a result of the episodic nature of stream migration were differentiated as follows. The proximal overbank sequences are composed of ripple-laminated (lithofacies Sr) and massive (lithofacies Smf) sandstone interbedded with fine-grained deposits (lithofacies Fs, Fm, and Fcsm) and calcisols (lithofacies P). The distal overbank depsits are predominantly mudstones that are entirely destratified mudstone (lithofacies Fm). Abandoned channel-fill deposits were also identified. These are composed of carbonaceous mudstone often contains fragments of unionid bivalve shells (lithofacies Fcsm), massive mudstone (lithofacies Fm), and coal (lithofacies C). Finally, some channel-fills contain fluvial tufas which exhibit pseudo-stromatolitic banding and include fossil ostracodes and charophytes (lithofacies Lm). The fluvial gravels (lithofacies Gm, Gt, and Gp) often contain eroded tufa clasts. The ten measured stratigraphic sections encompass several significant dinosaur localities which contain at least 11 individuals, greater that one hundred Allosaurus teeth, thousands of individual bones, tracks, and coprolites. Several partial specimens have been excavated from abandoned channel sequences interpreted as former (wetlands or bogs), also individual abraded bones can be found in fluvial channel sequences. The transition up-section from the localities of abundant dinosaur remains, “lower Brushy Basin Member”, to somewhat barren intervals, “upper Brushy Basin Member”, coincides with a distinct change in fluvial style from isolated, lenticular, single-story channels encased in thick grey floodplain sequences with abundant, but, thin paleosols, “lower Brushy Basin Member”, to laterally continuous channel belts surrounded by a more reddish floodplain sequences with relatively thicker composite paleosols. The Brushy Basin Member can be informally spilt into a lower units characterized by a change in color and fluvial style is interpreted to indicate a change in sedimentation accumulation rates, from higher accumulation rates to lower accumulation rates. The taphonomic implications are as follows. The lower unit favored fossil preservation because of the higher sedimentation rates, while the upper unit favored weather which resulted from a lower sedimentation rates. This change in accumulation rates, which resulted in the obvious transition in fluvial style, could have been a product of a change in base level, tectonics, or possibly a sediment supply/paleoclimate change. This study also interpreted the paleoclimate of this vertebrate fossil rich locality based on types of paleosols identified, such as calcisols, gleysols, and paleo-histosols. The local climate in this area during the late Jurassic was extremely seasonal having distinctive “wet” and “dry” periods.