Abstract: A well-preserved record of phosphatic sedimentation across an ancient continental ramp is contained in Upper Leonardian–Guadalupian (Upper Permian) strata of the Phosphoria and Park City Formations exposed along the flanks of the Uinta Mountains, northeastern Utah. The Uinta Mountain exposures trend approximately down depositional dip and, unlike exposures of the type Phosphoria in the Idaho–Wyoming overthrust belt, are not structurally telescoped. This study is based on 12 detailed measured sections and hundreds of samples collected and studied macroscopically and microscopically from the uppermost Grandeur Member (Park City Formation), Meade Peak Member (Phosphoria Formation), and Franson Member (Park City Formation). The uppermost Grandeur Member is characterized by local carbonate hardgrounds, which are partially reworked in a transgressive lag at the base of the Meade Peak. Strata from the Meade Peak and Franson are described in terms of five lithofacies: 1) organic-rich dolomite, which is fine-grained, laminated, and present only in distal sections of the Meade Peak; 2) granular phosphorite packstone and grainstone, which is mainly associated with the Meade Peak and consists of peloids, phosphatic shelly debris, intraclasts, molluscan steinkerns, and local phosphatic coated grains; 3) gray shale; and 4) chert, which are most common at the transition zone between the Meade Peak and Franson Members; and 5) phosphatic dolowackestone, which comprises most of the Franson and which contains calcite-filled molds after anhydrite nodules and supratidal fabrics in more shoreward sections. Stratal architecture and stacking patterns, as well as the sedimentologic character and degree of bioturbation of individual facies, suggest that the Meade Peak and Franson members together are unconformity bounded and record a single major transgressive-regressive cycle. As such, they are interpreted as a stratigraphic sequence. In addition, detailed sedimentologic relations suggest that repetitively interbedded phosphorite, gray shale, and phosphatic dolowackestone of the transition zone between the Meade Peak and Franson were deposited in response to small-scale fluctuations in sea level, likely with associated changes in climate that affected the ramp. The nature and style of phosphate accumulation were not uniform across the ramp, but varied down depositional dip. Poorly oxygenated basin–ward positions were marked by deposition of organic-rich carbonate in which phosphate is interpreted to have grown authigenically in situ . In contrast, the inner ramp was current-winnowed, well oxygenated, and was the site of phosphate condensation, as suggested by the presence of only minor amounts of interstitial mud, the ubiquity of bioturbation, and the abundance of granular phosphorite, respectively.