Outer platform carbonates of the Lower to Middle Cambrian Shady Dolomite, Virginia Appalachians, record a lengthy and complex diagenetic history, ranging from marine cementation to burial diagenesis during late Paleozoic overthrusting. Analysis of petrographically well-preserved marine cements has provided an estimate of the isotopic composition of Lower Cambrian marine carbonate (delta 18 O = -7.5 to -6.1 per thousand PDB; delta 13 C = +0.2 to +0.8 per thousand PDB; 87 Sr/ 86 Sr = 0.70869 to 0.70975), establishing a base line with which to assess later diagenetic carbonates. Meteoric dissolution and early calcite cement postdate marine cementation and formed during subaerial exposure. The platform margin carbonates were extensively dolomitized; dolomitization postdates calcite cementation and the initial development of stylolites and tectonic fractures. Several episodes of dolomite replacement and cementation are evident. Zone 1 dolomite consists of rare relict dolomite cores which were replaced and overgrown by zone 2A dolomite, the dominant replacement phase. Zone 2A dolomite is depleted in 18 O (delta 18 O = -10.2 to -7.0) and enriched in 13 C (delta 13 C = +1.0 to +1.6) relative to marine carbonate, reflecting precipitation from warm formation fluids buffered by the host carbonate. Uniformly low Sr contents (25 to 65 ppm) and nonradiogenic 87 Sr/ 86 Sr (0.70900 to 0.70971) also attest to pore water equilibration with the host rock. Replacement dolomitization was followed by widespread carbonate dissolution, which formed vuggy porosity and local solution breccias. The host dolomite locally is encrusted by Mississippi Valley-type (MVT) occurrences of ore mineralization consisting of sphalerite, galena, and pyrite. This major generation of ore minerals is overgrown by three generations of dolomite cement. The first dolomite cement, zone 2B, has similar 18 O composition (delta 13 O = -10.3 to -7.4) but slightly depleted 13 C values (delta 13 C = +0.4 to +1.1) relative to zone 2A dolomite and has similar Sr contents (30 to 45 ppm) and 87 Sr/ 86 Sr ratios (0.70933 to 0.70966). Zone 2B dolomite cement exhibits petrographic, isotopic, and geochemical affinities with zone 2A replacement dolomite, implying that the two dolomite types formed from fluids of similar composition and temperature. Primary fluid inclusions in zone 2B dolomite indicate precipitation from warm (minimum 120 to 150 degrees C) brines (23-26 wt. % NaCl equiv.). These temperatures imply that the dolomitizing fluid was enriched in 18 O due to extensive water-rock interaction with host carbonate, which also buffered the fluid delta 13 C, Sr, and 87 Sr/ 86 Sr content. Zones 3 and 4 dolomite cement are depleted in 18 O (delta 13 O = -13.8 to -11.3) relative to the previous dolomites, implying a temperature increase to 150 to 210 degrees C. The late dolomite cements have 13 C compositions (delta 13 C = -0.7 to +0.9) ranging from those similar to the earlier dolomites to more depleted values. Zones 3 and 4 dolomite cement are enriched in Sr (60 to 135 ppm) which is radiogenic ( 87 Sr/ 86 Sr = 0.71025 to 0.71445). These later cements thus record fluids that were no longer buffered by the host carbonate. Dolomite cements locally were overgrown by sphalerite, followed by authigenic quartz and calcite cement. Secondary three phase fluid inclusions in quartz and calcite indicate hot (175 to 225 degrees C) saline (30 to 33 wt. % NaCl equiv.) fluids. Temperatures and pressures interpreted from the fluid inclusions are compatible with estimated burial depths in excess of 5 km. The dolomites formed during deep burial, coeval with late Paleozoic, Alleghanian-age thrusting. The Mg required for burial dolomitization was derived from pressure solution of structurally lower, platform interior dolomites that were overridden by the Shady Dolomite thrust sheet. Tectonic uplift and deformation resulted in regional fluid flow, which transported this Mg to the Shady Dolomite outer platform during burial dolomitization.