T235 Ocean Chemistry through the Precambrian and Paleozoic II

Wednesday, 10 November 2004
1:30 PM - 5:30 PM

LOWER MISSISSIPPIAN POSITIVE CARBON ISOTOPE EXCURSION IN SHALLOW WATER CARBONATES, WYOMING AND MONTANA

Paper number: T235-12
Program: Technical Sessions
Time: 4:00 PM – 4:15 PM

Authors

Abstract

Lower Mississippian carbonates from Wyoming and Montana show a positive carbon isotope excursion (δ13C values range from +5 to +7.5 ‰ PDB) within North American-Lower Mississippian/Kinderhookian to Osagean (Tournasian to Lower Visean) intervals, indicating a fluctuation in the global carbon cycle at that time. This carbon isotope excursion is found along the entire Madison ramp in cores (Elk and Bighorn Basins) and in measured sections in Wyoming and Montana. The excursion is independent of facies and occurrs in pervasively dolomitized up dip locations as well as basinward locations composed entirely of limestone.

Positive carbon values are intimately associated with sequence stratigraphy previously determined in the measured sections. The onset of the transgression in Sequence II coincides with the most depleted carbon values (ca. 1 ‰ PDB) and a progressive increase of enrichment during the transgression. It reaches a maximum enrichment (ca. 7 ‰ PDB) at the turnaround to the regression, followed by a gradual trend from maximum values at the turnaround to minimum values (ca. 2 ‰ PDB) at the top of the sequence. On the Madison ramp, the positive carbon excursion can be used to correlate third order sequence boundaries across the 1100 km ramp system, providing a time line within otherwise undatable sections.

On a larger scheme, these enriched values also correlate to time-equivalent strata discovered in previous studies from Utah, Nevada, Idaho, Wyoming, Iowa, and Western Europe, indicating its potential use as a global chronostratigraphic tool. The timing of this event probably coincides with low atmospheric CO2 levels and the initiation of conditions that lead to the Icehouse Earth in the Upper Mississippian. In order to confirm this interpretation we are measuring the δ13C of coexisting organic material to compare the difference between δ13C of the inorganic and organic components and assess pCO2 levels and associated changes within the marine organic and inorganic carbon pools.