2014 GSA Annual Meeting in Vancouver, British Columbia (19–22 October 2014)

Paper No. 108-9
Presentation Time: 10:10 AM


JOST, Adam B., Department of Geological and Environmental Sciences, Stanford University, 450 Serra Mall, Building 320, Stanford, CA 94305, BACHAN, Aviv, Department of Geosciences, The Pennsylvania State University, 510 Deike Building, University Park, PA 16802, VAN DE SCHOOTBRUGGE, Bas, Department of Earth Sciences, Utrecht University, Princetonlaan 8A, Utrecht, 3584 CB, Netherlands, DEPAOLO, Donald J., Earth and Planetary Science, University of California, Berkeley, 307 McCone Hall, Berkeley, CA 94720-4767 and PAYNE, Jonathan L., Department of Geological Sciences, Stanford University, 450 Serra Mall, Building 320, Stanford, CA 94305

The end-Triassic mass extinction preferentially affected heavily calcified marine animals, suggesting ocean acidification was an important kill mechanism. Carbon isotope fluctuations across the Triassic-Jurassic boundary and into the Lower Jurassic are consistent with input of volcanic CO2 from the Central Atlantic Magmatic Province (CAMP) as an underlying driver. However, changes in δ13C cannot be uniquely attributed to volcanic carbon release, and the ocean acidification scenario has yet to be tested using other geochemical proxies. Here we present a high-resolution calcium isotope record from 100 m of marine carbonate sediments spanning the Triassic-Jurassic boundary in two stratigraphic sections from the Lombardy Basin of the southern Alps. Just above the Triassic-Jurassic boundary and the 6‰ negative δ13C excursion, δ44/40Ca decreases approximately 0.7‰ over less than 20 m, then recovers by 0.8‰ over the next 20 m. There are several potential controls on the δ44/40Ca of limestone, including the δ44/40Ca of seawater, carbonate mineralogy, precipitation rate, groundwater discharge, and early diagenesis. The most plausible local control is a fluctuation in the proportion of calcite and aragonite sediment being produced locally. Whereas this mechanism can account for variations in δ44/40Ca, it does not explain the coupled variation in δ44/40Ca and δ13C, the coeval mass extinction event, or the evidence for climate warming. Overall, the most parsimonious explanation for the coupled behavior of the carbon and calcium isotope data is that elevated CO2 emissions from CAMP volcanism resulted in perturbations to the global carbon and calcium cycles via ocean acidification and enhanced continental weathering. Coupled numerical modeling of the carbon and calcium cycles demonstrates that the δ13C and δ44/40Ca records can reflect the input of large volumes of CO2 during emplacement of CAMP and gives us quantitative constraints on the volume and isotopic composition of emitted CO2. This acidification scenario also explains the selective extinction of marine calcifiers, the temporary reduction in carbonate deposition, and the evidence for fluctuating pCO2 during the end-Triassic crisis.