An oxygen isotope model for interpreting carbonate diagenesis in nonmarine rocks (Green River Basin, Wyoming, USA)

Abstract

A closed-system model is used for predicting the δ18O of formation waters in the deep portions of the northern Green River basin, Wyoming. δ18Ocalcite is calculated from this modeled water and compared with the δ18O of measured calcites to help interpret diagenesis in the basin. The modification of 18Owater, which may be caused by diagenetic reactions at elevated temperatures, is modeled from two mass-balance equations. Three diagenetic reactions used to modify δ18Owater include: detrital limestoneå calcite cement; detrital quartz→ quartz cement; and detrital clay å authigenic illite/smectite. A weighted average δ18Owater and δ18O of calcite, quartz and illite/smectite in equilibrium with this water are calculated at 500-m increments. For a closed-system model, calculated variables at one depth are used for input variables at the next depth. An open system can be crudely simulated by adjusting the input variables at each depth. Petrographic and hydrologic data suggest that throughout much of the basin an open hydrochemical system overlies a relatively closed system which is below 3000 m. From the surface to 3000 m deep, δ18Ocalcite measured in sandstone cements deviates from calculated 18Ocalcite for the closed-system model. Below 3000 m, δ18Ocalcite of cement and bulk shale converge from opposite directions with increasing depth toward the calculated δ18Ocalcite. Adjusting the calculated δ18Ocalcite to match the measured δ18Ocalcite indicates that the deviation above 3000 m results from mixing of meteoric waters with 18O-rich formation water.