Abstract
Oceanic Anoxic Event 2 (ca. 94 Ma; OAE2) was one of the largest Mesozoic carbon cycle perturbations, but associated carbon emissions, primarily from the Caribbean large igneous province (LIP) and marine burial fluxes, are poorly constrained. Here, we use the carbon cycle box model LOSCAR-P to quantify the role of LIP volcanism and enhanced marine organic carbon (Corg) burial as constrained by the magnitude and shape of the positive stable carbon isotope (δ13C) excursion (CIE) in the exogenic carbon pool and atmospheric pCO2 reconstructions. In our best fit scenario, two pulses of volcanic carbon input—0.065 Pg C yr–1 over 170 k.y. and 0.075 Pg C yr–1 over 40 k.y., separated by an 80 k.y. interval with an input of 0.02 Pg C yr–1—are required to simulate observed changes in δ13C and pCO2. Reduced LIP activity and Corg burial lead to pronounced pCO2 reductions at the termination of both volcanic pulses, consistent with widespread evidence for cooling and a temporal negative trend in the global exogenic δ13C record. Finally, we show that observed leads and lags between such features in the records and simulations are explained by differences in the response time of components of the carbon cycle to volcanic forcing
| Original language | English |
|---|---|
| Pages (from-to) | 511-515 |
| Number of pages | 5 |
| Journal | Geology |
| Volume | 50 |
| Issue number | 4 |
| DOIs | |
| Publication status | Published - 1 Apr 2022 |
Bibliographical note
Funding Information:This research was funded by The Netherlands Earth System Science Center (NESSC), which is financially supported by the Dutch Ministry of Education, Culture and Science; a NESSC Travel Grant; and the European Research Council (Starting Grant 278364 to C. Slomp, and Consolidator Grant 771497 to A. Sluijs). We thank R. Zeebe and N. Komar, University of Hawai’i, for the LOSCAR-P code and advice. H. Pälike was supported through the Cluster of Excellence “The Ocean Floor–Earth’s Uncharted Interface” (research unit recorder), DFG 390741603. We thank M. Jones, I. Jarvis, and J. Owens for their helpful reviews and comments
Funding Information:
This research was funded by The Netherlands Earth System Science Center (NESSC), which is financially supported by the Dutch Ministry of Education, Culture and Science; a NESSC Travel Grant; and the European Research Council (Starting Grant 278364 to C. Slomp, and Consolidator Grant 771497 to A. Sluijs). We thank R. Zeebe and N. Komar, University of Hawai’i, for the LOSCAR-P code and advice. H. Pälike was supported through the Cluster of Excellence “The Ocean Floor–Earth’s Uncharted Interface” (research unit recorder), DFG 390741603. We thank M. Jones, I. Jarvis, and J. Owens for their helpful reviews and comments.
Publisher Copyright:
© 2022 Geological Society of America
Funding
This research was funded by The Netherlands Earth System Science Center (NESSC), which is financially supported by the Dutch Ministry of Education, Culture and Science; a NESSC Travel Grant; and the European Research Council (Starting Grant 278364 to C. Slomp, and Consolidator Grant 771497 to A. Sluijs). We thank R. Zeebe and N. Komar, University of Hawai?i, for the LOSCAR-P code and advice. H. P?like was supported through the Cluster of Excellence ?The Ocean Floor?Earth?s Uncharted Interface? (research unit recorder), DFG 390741603. We thank M. Jones, I. Jarvis, and J. Owens for their helpful reviews and comments This research was funded by The Netherlands Earth System Science Center (NESSC), which is financially supported by the Dutch Ministry of Education, Culture and Science; a NESSC Travel Grant; and the European Research Council (Starting Grant 278364 to C. Slomp, and Consolidator Grant 771497 to A. Sluijs). We thank R. Zeebe and N. Komar, University of Hawai’i, for the LOSCAR-P code and advice. H. Pälike was supported through the Cluster of Excellence “The Ocean Floor–Earth’s Uncharted Interface” (research unit recorder), DFG 390741603. We thank M. Jones, I. Jarvis, and J. Owens for their helpful reviews and comments.
