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Enhanced continental chemical weathering during the multiple early Eocene hyperthermals: New constraints from the southern Indian Ocean

Tanaka, Erika, Yasukawa, Kazutaka, Ohta, Junichiro, Kato, Yasuhiro·2022·Geochimica et Cosmochimica Acta
DOI 10.1016/j.gca.2022.05.022
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Fig. 1 (a) Paleogeographic map showing the locations of the sites and LIPs considered in this study at 55 Ma, modified from Yasukawa et al. (2017), Wells et al. (2014), and Wilkinson et al. (2017). The map was created by using GPlates software (http://www.gplates.org) version 1.2.0 with the EarthByte Global Rotation Model62 and the Global Time-Dependent Age Grid63, and Generic Mapping Tools software (https:// www.soest.hawaii.edu/gmt/), version 4.5.8 (Wessel and Smith, 1998). (b) High-resolution benthic d 18 O ( Nuttallides truempyi ) records from Ocean Drilling Program (ODP) Site 1209 and Site 1262/1263 (Westerhold et al., 2018, 2020) with the active age intervals of the North Atlantic Igneous Province (NAIP) and Siletzia (Storey et al., 2007; Wells et al., 2014; Wilkinson et al., 2017). (c) High-resolution benthic d 13 C ( Nuttallides truempyi ) records from ODP Sites 1209 and 1262/1263 (Westerhold et al., 2018, 2020) with bulk d 13 C records from ODP Site 752 (Yasukawa et al., 2017).
Fig. 1 (a) Paleogeographic map showing the locations of the sites and LIPs considered in this study at 55 Ma, modified from Yasukawa et al. (2017), Wells et al. (2014), and Wilkinson et al. (2017). The map was created by using GPlates software (http://www.gplates.org) version 1.2.0 with the EarthByte Global Rotation Model62 and the Global Time-Dependent Age Grid63, and Generic Mapping Tools software (https:// www.soest.hawaii.edu/gmt/), version 4.5.8 (Wessel and Smith, 1998). (b) High-resolution benthic d 18 O ( Nuttallides truempyi ) records from Ocean Drilling Program (ODP) Site 1209 and Site 1262/1263 (Westerhold et al., 2018, 2020) with the active age intervals of the North Atlantic Igneous Province (NAIP) and Siletzia (Storey et al., 2007; Wells et al., 2014; Wilkinson et al., 2017). (c) High-resolution benthic d 13 C ( Nuttallides truempyi ) records from ODP Sites 1209 and 1262/1263 (Westerhold et al., 2018, 2020) with bulk d 13 C records from ODP Site 752 (Yasukawa et al., 2017).CC-BY · From the PDF
Image 2
CC-BY · From the PDF
Fig. 2 Estimated proportions of Os isotopes in (a) continental silicate with ( 187 Os/ 188 Os)silw = 1.4 and (b) mantle-origin components with ( 187 Os/ 188 Os)mo = 0.12. In the estimation, we assumed that the mass abundance ratios of 188 Os: 184 Os, 188 Os: 186 Os, 188 Os: 189 Os, 188 Os: 190 Os, and 188 Os: 192 Os are constant because they are stable isotopes, and that the mass abundance ratio of 188 Os: 187 Os could be different in continental silicate and mantle-origin components. The reported values of representative isotopic abundances for Os are from Meija et al. (2016): 0.02% for 184 Os; 1.59% for 186 Os; 13.24% for 188 Os; 16.15% for 189 Os; 26.26% for 190 Os; and 40.78% for 192 Os. Using the assumed 187 Os/ 188 Os values and the representative isotopic abundances noted above, we estimated all Os isotope abundances in (a) and (b).
Fig. 2 Estimated proportions of Os isotopes in (a) continental silicate with ( 187 Os/ 188 Os)silw = 1.4 and (b) mantle-origin components with ( 187 Os/ 188 Os)mo = 0.12. In the estimation, we assumed that the mass abundance ratios of 188 Os: 184 Os, 188 Os: 186 Os, 188 Os: 189 Os, 188 Os: 190 Os, and 188 Os: 192 Os are constant because they are stable isotopes, and that the mass abundance ratio of 188 Os: 187 Os could be different in continental silicate and mantle-origin components. The reported values of representative isotopic abundances for Os are from Meija et al. (2016): 0.02% for 184 Os; 1.59% for 186 Os; 13.24% for 188 Os; 16.15% for 189 Os; 26.26% for 190 Os; and 40.78% for 192 Os. Using the assumed 187 Os/ 188 Os values and the representative isotopic abundances noted above, we estimated all Os isotope abundances in (a) and (b).CC-BY · From the PDF
Fig. 3 Calculated 187 Os/ 188 Os results of a simple two-component mixing model [continental silicate with ( 187 Os/ 188 Os)silw of  1.4 and mantleorigin component with ( 187 Os/ 188 Os)mo of  0.12] based on Model 1 and Model 2. The proportion of mantle-origin components is changed from 0% to 100% or that of continental silicate weathering flux is changed from 100% to 0% in both Models 1 and 2.
Fig. 3 Calculated 187 Os/ 188 Os results of a simple two-component mixing model [continental silicate with ( 187 Os/ 188 Os)silw of  1.4 and mantleorigin component with ( 187 Os/ 188 Os)mo of  0.12] based on Model 1 and Model 2. The proportion of mantle-origin components is changed from 0% to 100% or that of continental silicate weathering flux is changed from 100% to 0% in both Models 1 and 2.CC-BY · From the PDF
Fig. 4 Data summary of the lower Eocene sequence of ODP Site 752. The 187 Os/ 188 Os i values and Os burial flux are newly reported in this study. The core information (e.g., lithology, sediment color, magnetic polarity, and nannofossil zones), carbon isotope ratios ( d 13 Ccarb), and CaCO3 contents of bulk carbonate are from the ODP Initial Report (Shipboard Scientific Party, 1989; Seto et al. (1991)) and Yasukawa et al. (2017). Sediment burial flux was calculated in this study based on the ODP Initial Report (Shipboard Scientific Party, 1989) and Yasukawa et al. (2017), as described in Text S1 and Table S1. The horizontal pink and blue bars indicate the carbon isotope excursions corresponding to the hyperthermal events and the pre-ETM3 interval. The uncertainty (2 S.E.) of 187 Os/ 188 Os i is given within each symbol; note that the uncertainties are smaller than the symbols.
Fig. 4 Data summary of the lower Eocene sequence of ODP Site 752. The 187 Os/ 188 Os i values and Os burial flux are newly reported in this study. The core information (e.g., lithology, sediment color, magnetic polarity, and nannofossil zones), carbon isotope ratios ( d 13 Ccarb), and CaCO3 contents of bulk carbonate are from the ODP Initial Report (Shipboard Scientific Party, 1989; Seto et al. (1991)) and Yasukawa et al. (2017). Sediment burial flux was calculated in this study based on the ODP Initial Report (Shipboard Scientific Party, 1989) and Yasukawa et al. (2017), as described in Text S1 and Table S1. The horizontal pink and blue bars indicate the carbon isotope excursions corresponding to the hyperthermal events and the pre-ETM3 interval. The uncertainty (2 S.E.) of 187 Os/ 188 Os i is given within each symbol; note that the uncertainties are smaller than the symbols.CC-BY · From the PDF
Fig. 5 Percentage increases in continental silicate weathering during hyperthermal events.
Fig. 5 Percentage increases in continental silicate weathering during hyperthermal events.CC-BY · From the PDF

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Cited by

See all 17

Metadata

Authors
Tanaka, E., Yasukawa, K., Ohta, J., & Kato, Y.
Venue
Geochimica et Cosmochimica Acta
Publisher
Elsevier BV
Published
2022-08
Volume
331
Pages
192-211
ISSN
0016-7037
DOI
10.1016/j.gca.2022.05.022
Cited by
17
References
0
Language
en
Licence
Funders
  • Japan Society for the Promotion of Science (JP15H05771, JP18J22633, JP20H02678, JP20H05658, JP21J00998)
  • University of Tokyo

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CoChat. (2026). Citation check: Enhanced continental chemical weathering during the multiple early Eocene hyperthermals: New constraints from the southern Indian Ocean. https://app.cochat.ai/papers/10.1016/j.gca.2022.05.022
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Tanaka, E., Yasukawa, K., Ohta, J., & Kato, Y. (2022). Enhanced continental chemical weathering during the multiple early Eocene hyperthermals: New constraints from the southern Indian Ocean. Geochimica et Cosmochimica Acta. https://doi.org/10.1016/j.gca.2022.05.022