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An evaluation of Deccan Traps eruption rates using geochronologic data

Schoene, Blair, Eddy, Michael P., Keller, C. Brenhin, Samperton, Kyle M.·2021·Geochronology
DOI 10.5194/gchron-3-181-2021

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Abstract

Recent attempts to establish the eruptive history of the Deccan Traps large igneous province have used both U−Pb (Schoene et al., 2019) and 40Ar/39Ar (Sprain et al., 2019) geochronology. Both of these studies report dates with high precision and unprecedented coverage for a large igneous province and agree that the main phase of eruptions began near the C30n–C29r magnetic reversal and waned shortly after the C29r–C29n reversal, totaling ∼ 700–800 kyr duration. These datasets can be analyzed in finer detail to determine eruption rates, which are critical for connecting volcanism, associated volatile emissions, and any potential effects on the Earth's climate before and after the Cretaceous–Paleogene boundary (KPB). It is our observation that the community has frequently misinterpreted how the eruption rates derived from these two datasets vary across the KPB. The U−Pb dataset of Schoene et al. (2019) was interpreted by those authors to indicate four major eruptive pulses before and after the KPB. The 40Ar/39Ar dataset did not identify such pulses and has been largely interpreted by the community to indicate an increase in eruption rates coincident with the Chicxulub impact (Renne et al., 2015; Richards et al., 2015). Although the overall agreement in eruption duration is an achievement for geochronology, it is important to clarify the limitations in comparing the two datasets and to highlight paths toward achieving higher-resolution eruption models for the Deccan Traps and for other large igneous provinces. Here, we generate chronostratigraphic models for both datasets using the same statistical techniques and show that the two datasets agree very well. More specifically, we infer that (1) age modeling of the 40Ar/39Ar dataset results in constant eruption rates with relatively large uncertainties through the duration of the Deccan Traps eruptions and provides no support for (or evidence against) the pulses identified by the U−Pb data, (2) the stratigraphic positions of the Chicxulub impact using the 40Ar/39Ar and U−Pb datasets do not agree within their uncertainties, and (3) neither dataset supports the notion of an increase in eruption rate as a result of the Chicxulub impact. We then discuss the importance of systematic uncertainties between the dating methods that challenge direct comparisons between them, and we highlight the geologic uncertainties, such as regional stratigraphic correlations, that need to be tested to ensure the accuracy of eruption models. While the production of precise and accurate geochronologic data is of course essential to studies of Earth history, our analysis underscores that the accuracy of a final result is also critically dependent on how such data are interpreted and presented to the broader community of geoscientists.

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Figures

Fig. 1 Geography and stratigraphy of the Deccan Traps in the Western Ghats Region. a) Map of India (© Google Earth), showing in red the footprint of the Deccan Traps; white box indicates the study area, called the western Ghats, enlarged in (b). b) Colored relief map (© OpenStreetMap contributors 2020. Distributed under a Creative Commons BY-SA License) of 620 the Western Ghats showing several cities and cross-section line from (d). c) Stratigraphic column of the major basalt unit subdivisions in the Western Ghats. Stratigraphy measured as cumulative volume, using the volume model for each formation from (Richards et al., 2015), which was used in both Schoene et al. (2019) and Sprain et al. (2019). d) Cross section through the Western Ghats. Cross-section line chosen to go through the sampling sites in Schoene et al. 625 (2019). All figures modified from Schoene et al. (2015), Schoene et al. (2019), and references therein.
Fig. 1 Geography and stratigraphy of the Deccan Traps in the Western Ghats Region. a) Map of India (© Google Earth), showing in red the footprint of the Deccan Traps; white box indicates the study area, called the western Ghats, enlarged in (b). b) Colored relief map (© OpenStreetMap contributors 2020. Distributed under a Creative Commons BY-SA License) of 620 the Western Ghats showing several cities and cross-section line from (d). c) Stratigraphic column of the major basalt unit subdivisions in the Western Ghats. Stratigraphy measured as cumulative volume, using the volume model for each formation from (Richards et al., 2015), which was used in both Schoene et al. (2019) and Sprain et al. (2019). d) Cross section through the Western Ghats. Cross-section line chosen to go through the sampling sites in Schoene et al. 625 (2019). All figures modified from Schoene et al. (2015), Schoene et al. (2019), and references therein.CC-BY · From the PDF
Image 2
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Fig. 2 Eruption rate model for the Deccan Traps, based on U-Pb geochronology. (A) Results from the MCMC algorithm used to generate the age model in Fig. 1, converted to a probabilistic volumetric eruption rate for the Deccan Traps shown with contours up to 68% credible intervals. The U-Pb date for the Chicxulub impact is the same as in Fig. 1. Total global volcanic productivity (~3-4 km³/year) includes mid-ocean ridges and volcanic arcs (28).
Fig. 2 Eruption rate model for the Deccan Traps, based on U-Pb geochronology. (A) Results from the MCMC algorithm used to generate the age model in Fig. 1, converted to a probabilistic volumetric eruption rate for the Deccan Traps shown with contours up to 68% credible intervals. The U-Pb date for the Chicxulub impact is the same as in Fig. 1. Total global volcanic productivity (~3-4 km³/year) includes mid-ocean ridges and volcanic arcs (28).CC-BY · From the PDF
Fig. 3 Recalculated eruption rates from Fig. 4 of Sprain et al. (2019). Original figure was converted to an eruption rate by dividing the total volume of each formation (the heights in their Fig. 4), by their estimated durations for each formation, to give units of km 3 /a. Time on the xaxis, and color and width of each box is left as from their original figure. See Fig. 4 of this paper for probabilistic eruption rates.
Fig. 3 Recalculated eruption rates from Fig. 4 of Sprain et al. (2019). Original figure was converted to an eruption rate by dividing the total volume of each formation (the heights in their Fig. 4), by their estimated durations for each formation, to give units of km 3 /a. Time on the xaxis, and color and width of each box is left as from their original figure. See Fig. 4 of this paper for probabilistic eruption rates.CC-BY · From the PDF
Image 5
CC-BY · From the PDF
Fig. 4 Age models and eruption rates for the Deccan Traps. Age models and eruptions rates produced using geochronologic data from Schoene et al. (2019; red) and Sprain et al. 650 (2019; blue), using the same methods as described in Schoene et al. (2019). Data and model for Schoene et al. (2019) are identical to those in the original publication. Note the units on the stratigraphy in the top panel are cumulative km 3 , not m, and so the slope of the age models are km 3 /a, which is plotted in the lower panel. Volume model is from Richards et al. (2015). Stratigraphic heights for the Sprain et al. (2019) samples are taken from their Fig. 2. Also plotted 655 is the probability of the stratigraphic position of the Chicxulub impact as calculated during the MCMC age modeling by querying where an accepted age model intersects an age for the KPg. U-Pb age model is compared to U-Pb KPg date from Clyde et al., (2016); 40 Ar/ 39 Ar age model is compared to 40 Ar/ 39 Ar KPg date from (Sprain et al., 2018).
Fig. 4 Age models and eruption rates for the Deccan Traps. Age models and eruptions rates produced using geochronologic data from Schoene et al. (2019; red) and Sprain et al. 650 (2019; blue), using the same methods as described in Schoene et al. (2019). Data and model for Schoene et al. (2019) are identical to those in the original publication. Note the units on the stratigraphy in the top panel are cumulative km 3 , not m, and so the slope of the age models are km 3 /a, which is plotted in the lower panel. Volume model is from Richards et al. (2015). Stratigraphic heights for the Sprain et al. (2019) samples are taken from their Fig. 2. Also plotted 655 is the probability of the stratigraphic position of the Chicxulub impact as calculated during the MCMC age modeling by querying where an accepted age model intersects an age for the KPg. U-Pb age model is compared to U-Pb KPg date from Clyde et al., (2016); 40 Ar/ 39 Ar age model is compared to 40 Ar/ 39 Ar KPg date from (Sprain et al., 2018).CC-BY · From the PDF
Image 7
CC-BY · From the PDF
Image 8
CC-BY · From the PDF
Fig. 6 Synthetic dataset subjected to MCMC age modeling to test the age precision 675 necessary to resolve pulses in eruptions. Upper left shows the dataset, meant to approximate the age model of Schoene et al. (2019), but shown here with negligible uncertainties (±10 ka 2sigma). Other panels show model outputs for eruption rates generated for different 2sigma uncertainties on the input data themselves (i.e., uncertainties on 'data' from upper left panel). The results indicate that a threshold of precision is required for geochronology 680 to resolve pulses and hiatuses of given durations. Also shown in red are the average reported 2sigma uncertainties on eruption ages from the U-Pb dataset of Schoene et al. (2019) and the 40 Ar/ 39 Ar dataset from Sprain et al. (2019). The point is that the lower precision 40 Ar/ 39 Ar dataset cannot possibly test the hiatus and pulse model observed by the U-Pb dataset.
Fig. 6 Synthetic dataset subjected to MCMC age modeling to test the age precision 675 necessary to resolve pulses in eruptions. Upper left shows the dataset, meant to approximate the age model of Schoene et al. (2019), but shown here with negligible uncertainties (±10 ka 2sigma). Other panels show model outputs for eruption rates generated for different 2sigma uncertainties on the input data themselves (i.e., uncertainties on 'data' from upper left panel). The results indicate that a threshold of precision is required for geochronology 680 to resolve pulses and hiatuses of given durations. Also shown in red are the average reported 2sigma uncertainties on eruption ages from the U-Pb dataset of Schoene et al. (2019) and the 40 Ar/ 39 Ar dataset from Sprain et al. (2019). The point is that the lower precision 40 Ar/ 39 Ar dataset cannot possibly test the hiatus and pulse model observed by the U-Pb dataset.CC-BY · From the PDF
Image 10
CC-BY · From the PDF
Image 11
CC-BY · From the PDF

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Metadata

Authors
Schoene, B., Eddy, M. P., Keller, C. B., & Samperton, K. M.
ORCID
Venue
Geochronology
Publisher
Copernicus GmbH
Published
2021-04-16
Volume
3
Issue
1
Pages
181-198
ISSN
2628-3719
DOI
10.5194/gchron-3-181-2021
Cited by
73
References
3
Language
en
Licence
creativecommons.org/licenses/by/4.0/ (vor)

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Schoene, B., Eddy, M. P., Keller, C. B., & Samperton, K. M. (2021). An evaluation of Deccan Traps eruption rates using geochronologic data. Geochronology. https://doi.org/10.5194/gchron-3-181-2021