Articles | Volume 10, issue 5
https://doi.org/10.5194/esurf-10-997-2022
https://doi.org/10.5194/esurf-10-997-2022
Research article
 | 
25 Oct 2022
Research article |  | 25 Oct 2022

The effects of late Cenozoic climate change on the global distribution of frost cracking

Hemanti Sharma, Sebastian G. Mutz, and Todd A. Ehlers

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Cited articles

Abe-Ouchi, A., Saito, F., Kageyama, M., Braconnot, P., Harrison, S. P., Lambeck, K., Otto-Bliesner, B. L., Peltier, W. R., Tarasov, L., Peterschmitt, J.-Y., and Takahashi, K.: Ice-sheet configuration in the CMIP5/PMIP3 Last Glacial Maximum experiments, Geosci. Model Dev., 8, 3621–3637, https://doi.org/10.5194/gmd-8-3621-2015, 2015. 
Acosta, V. T., Schildgen, T. F., Clarke, B. A., Scherler, D., Bookhagen, B., Wittmann, H., von Blanckenburg, F., and Strecker, M. R.: Effect of vegetation cover on millennial-scale landscape denudation rates in East Africa, Lithosphere, 7, 408–420, https://doi.org/10.1130/l402.1, 2015. 
Adams, B. A., Whipple, K. X., Forte, A. M., Heimsath, A. M., and Hodges, K. V.: Climate controls on erosion in tectonically active landscapes, Sci. Adv., 6, eaaz3166, https://doi.org/10.1126/sciadv.aaz3166, 2020. 
Amitrano, D., Gruber, S., and Girard, L.: Evidence of frost-cracking inferred from acoustic emissions in a high-alpine rock-wall, Earth Planet. Sc. Lett., 341–344, 86–93, https://doi.org/10.1016/j.epsl.2012.06.014, 2012. 
Andersen, J. L., Egholm, D. L., Knudsen, M. F., Jansen, J. D., and Nielsen, S. B.: The periglacial engine of mountain erosion – Part 1: Rates of frost cracking and frost creep, Earth Surf. Dynam., 3, 447–462, https://doi.org/10.5194/esurf-3-447-2015, 2015. 
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Short summary
We estimate global changes in frost cracking intensity (FCI) using process-based models for four time slices in the late Cenozoic ranging from the Pliocene (∼ 3 Ma) to pre-industrial (∼ 1850 CE, PI). For all time slices, results indicate that FCI was most prevalent in middle to high latitudes and high-elevation lower-latitude areas such as Tibet. Larger deviations (relative to PI) were observed in colder (LGM) and warmer climates (Pliocene) due to differences in temperature and glaciation.